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Les diagrammes suivants iilustrent la mithode. t 2 3 4 9 6 G AJ NORTH AMERICAN .^ '^MESOZOIC AND C^¥OZOIC Geology and Pateontology ; OR, AN ABRIDGP]D HISTORY OF OUR KNOWLEDGE OF THE TRIASSIO, JURASSIC, CRETACEOUS AND TERTIARY FORMATIONS OF THIS CONTINENT. r-% ■ Y\Q,'S.r, i^, 1 ^' ^ By S. A. MILLER. 1 1 ■■ . :- ' J ' > ' 5 » 1 • . T ) 3 ' .1 • 1 • • • ■ > 1 r » ' .1 * ' 1 > 1 4 CINCINNATI: , ' ■ . 1 PRINTED BY JAMES BARCLAY, 269 VINE STREET < .. ' ' 188x. PREFACE. This work is a historical review of what we know of the Triassic, Jurassic, Cretaceous and Tertiary formations of North America. It is not exhaustive, yet it contains more information in regard to these formations than will be found in any other single publication. In compiling the work, the language of the various authors, whose books are referred to, has been used wherever practicable, and when it has been abridged the substance has not been changed. The author has not had an opportunity to specially study any of these formations be- yond that part which is embraced within the period of the drift. The latter he has explored and studied, in its distribution, over many cf the States and a considerable part of Canada. He has undertaken to overthrow the glacial hypothesis, and now submits the facts and the conclusions he has drawn to the learned of this country and of Europe, and asks for their verdict. There is this further fact to be remembered. If there was no glacial period in North America, there was none in Europe. Only a limited number of copies of the book has been published in this form, though it has appeared, in parts, in the last three volumes of the Journal op the Cincinnati Society of Natural History. 'I 2*^40 6" IMH From the Journal of *he Cincinnati Society oj Xatural HiHtorij, October, 1879. NORTH AMERICAN MESOZOTC AND CJENOZOtC GEOLOGY AND PALAEONTOLOGY. By S. A. MiLLEU, Esq. The sciences of Geology and Puliiiontology had not advanced many stops, in Europe, before their growth had coinineneed in America. Their development, therefore, has been nearly contemporaneous in the two countries, though more rapid in the early part of the centur}-^ in the Old World than in the New. Europe has had William Smith, J. S. Miller, Sowerb}', Murchison, Lyell, Brongniart, D'Orbigny, Gold- fuss, Sternberg, Barrande, and many other distinguished authors; while America has had McCluro, Morton, Vanuxem, Hitchcock, Con- rad, Leidy, Hall, Lesquereux, Logan, Billings, Dawson, and others, or- iginal discoverers, who possessed the philosophical learning necessary for the correct application of the discov cries to the advancement and growth of the sciences. The facts, however, upon which these sciences are based, and which constitute the superstructure, as now understood, have been ascertained, so recentl}-, that one would hardly undertake to enumerate a score of the principal fathers of them, in either country, without mentioning the names of some who are still living. The first society organized for the advancement of science in Nortls America, of which we have any account, is the American Philosophical Society, instituted in 17fi9, in Philadelphia. The earliest geological papers that seem to be worth mentioning, appeared in the Transactions of this Society, and though its publications have not been rapid, they continue to appear, and to hold a high rank, whether devoted to Geologj', Palaeontology, or other departments of science. The society is indebted for its organization to Benjamin Franklin. The first volume of the Transactions appeared, in quarto, in 1771. mgggggm fa" Mesozoio and Cwnozoic GcoUxjn tnid PaloBontoUxjy, Belknap wrote, upon the VVIiite MoiintiiiuH, in 1781; Friitrliiiis, on the Rock and Casciido of the Yonghiogheny, in 178(); Willianj Dunbar, on large nianinialian bones found in Louisiana, a set of hunum teeth found while digging a well at the depth of 30 to 35 feet; and on the Mississippi river and its delta, in 1804, which was continued in 1809. B. II. Latrobe described the freestone quarrit's on the Potoujac and Rappahannock, in 1809; and William McClure, in the same year, pub- lished his Observations on the Geology of the United States, exi)la:ia- tory of a geological map. He divided the formations int() four classes, viz: 1st, Primitive rocks; 2d, Transition rocks; 3d, FUetz or Secondary rocks; and 4th, Alluvial rocks. These classes ho separated on their mineralogical characters, and ho treated oftluur dip and extent, as far as his observations permitted. And Thoinas Jefferson, who had been President of the United States, described the fossil bones of the Megalonyx, in 1818. The American Academy of Art;^ and Sciences was established in Boston, and commenced the publication of its Memoirs in 1780. The Academy of Natural Sciences, of Philadelphia, originated in 1812, but commenced its publications in 1817. It soon collected an extensive library of woiks upon Natural History, largely owing to the fine dona- tion by the generous and distinguished geologist, William ]McClure, and at once entered the field as an active society, alive to the im- portance of the publication of facts, as distinguished from theoretical considerations. Its publicatious, from the commencement, have oc- cupied the first rank in science, and are now, absolutely, indispensa- ble to every American naturalist, and should occupy a shelf in every public library. An idea of the absence -^f geological information, in this country, in 1803, may be formed when it is remembered that geology was not separated as a science from mineralogy, and that so little was known of mineralogy that it could hardly have ranked as a science ; for later in life, Prof. Silliman, speaking of this period, says, "it was a matter of extreme difflculty to obtain, among ourselves even, the names of the most common stones and minerals; and one might inquire earnestly, and long, before he could find any one to identify even quartz, feld- spar, or hornblende, among the simple minerals; or granite, porphyry, or trap, among the rocks. We speak from experience, and well re- member with what impatient, but almost despairing curiosity, we eyed the bleak, naked ridges, which impended over the valleys and plains that were the scenes of our youthful excursions. In vain did we doubt that the glittering spangles of mica, and the still more alluring bril- Jfesozoic and Cd-tHtzoir Oeoltiffif and PilifonffdiKjy. :i liancy ariiel, and l)y (jiiarlz, proved tlial these luiiierals were the ium, 0. iiigens, now Tridentipes ingens, 0. diversus, now Tridentipss elegans, O. minirmis, now Argo- zoum minimum., O. palmatus^ and 0. ietradactylus. In 1839, Prof H. D. Rogersf described the Red Sandstone of Penn- S3'lvania, which stretches through the central and northern portions in a long and irregular tract, from New Jersey to Maryland. It is found in the vicinity of Reading, and near the Potomac river, from which place is quarried the famous Red Sandstone used in Wash- ington city. Prof Rogers proposed to call this the " JMiddle Sec- ondary Red Sandstone formation," because it is higher than the Coal Measures, and below the Cretaceous Green Sand of New Jersey. In 1841, W. C. Rodlieldj described, from the Connecticut Valley, Fal- ceoniscus macropterus, now Ischyptenis inacrr oterus, P. agassizi, P. ovatus, Catoptenis anguilliform.is, C. parvnlus, and C. macrurus, now Diciyopyge macriira. In the same year. Prof Hifcchcocli;§ said the New Red Sandstone, extending from New Haven to the north line of INIass., in Northfield, occupies a narrow s^Miclinal trough, having a width of about 20 miles, from East Hampton, in Massachusetts, to the Sound at New Haven; but from P^ast Hampton to Northfield a width of only G or 7 miles. He described Fiiooi'des Gonneciicucensis, F. shepardi., Sauroidichnites harratti, S. heleroclitus, now Ancyropus '!ieteroclitus,8. minitans, now Plectropterna minitans, S. longipes, S. palmatas., and S. polemarchus, now Polemarchus gigas. He used the word Sauroidichnites as a gen- eric name, but described it as the name of a suborder under the class Ichnolite. He also described Omithoidichnites as a sub-order, and used it as a generic name, and described numerous species under it. These names have, however, been abandoned, and the species have also been abandoned or referred to genera properly defined. The '■' Am. Jour. Sei. and Arts, vol. xxix. t 3d Ann. Rep., Pa, X Am. Jour. Sci. and Arts, vol. xli. § Geo. of Mass. Mesozoic and Camozoic Geology and Paloiontoloyy. 9 Ornithoid ichnites are 0. giganteus, 0. tuberosus, 0, expansus, 0. cune- atus, 0. parvulus, O. ingens, 0. elegaus, O. deani, 0. tenuis, 0. macro- dactylus, O. divaricatus, 0. isodactyltis, O, delicatulus, 0. minimus, 0. gracilior, aud 0. tetradactylas. He afterward, l)efore the Association of American Geologists and Naturalists, described some species under these names, which he subsequently referred to other genera. In J 842, Prof. J. G. Percival* described the existence of these rocks in two places in Connecticut, as follows: The larger secondary' formation extends from Morris Cove, on the east side of New Haven Harbor, on the south, to the north end of North- field village, in Mass., on the north, a distance of nearly 80 miles. Its greatest width, near the central part of the basin, exceeds 20 miles. This basin is entirel}- surrounded by Primary rocks, except at New Haven Harbor, where, however, Primary rocks form the two points on the opposite sides of the basin. The smaller secondary formation ex- tends 6 to 7 miles from south to north, and at its widest point scarcely exceeds two miles in breadth, and is about equally included in the towns of Woodbury and Southbur3^ It forms a small isolated tract, nearly in the center of that part of the Western Primary, within the limits of the State, and nearly 15 miles west of the larger seconda'y formation. The rocks of both these formations consist of Red Sand- stones, Conglomerates and Shales, and the physical characters and organic remains indicate a peculiar relation to the New Red Sandstone of Europe. In 1843, Prof. W. W. Matherf described these rocks in the State of New York, as follows : The New Red Sandstone occupies that portion of Rockland county, from Grassy point along the base of the Highlands to New Jersey, and eastward to the Hudson, but a portion of its area is covered over by trap rocks. It has also been found in a small area in Richmond county. In color, it varies from chocolate brown, through brick-red and gra}' to white; in texture, it varies from pebbly conglomerate, through common sandstone, fissile and micaceous sandstone, to shale; and in composition, from perfectly siliceous to an argillo-calcareous marl. Where the trappean rocks have cut through the strata, or have spread laterall}' between them, their texture and appearance are much modified, and appear to have been subjected to the action of heat, which has partly melted them, or rendered them more compact and hard, like a hard-burnt brick, or has made them metalliferous. * Geo. of Conn. t Geo. of N. Y. 10 Mesczoic and Cmnozoic Geology and Pi>,la'.ontology. In the same year, Prof. W. B. Rogers* described, from the Trias of Eastern Virginia, Equisefum arumliniforme^ Calamites planicostnttts, Tceniopteris magnifolia, Zmnites obtusifolins, and Z. tenuistriatus. In 1847, Sir Charles L3'ellf described the Triassic coal field, on the James river, near Richmond, Virginia, as follows: The tract of country occupied by the crystalline or hypogene rocks, which runs parallel to the Alleghany mountains, and on their eastern side is in this part of Virginia about 70 miles broad; in the midst of this space the coal-field occurs in a depression of the granitic and other hypogene rocks, on which the coal resfs, and by which it is surrounded, along its outcrop. The length of the coal-field, from north to south, is about 26 miles, and its breadth varies from 4 to 12 miles. The James river flows through the middle of it, about 15 miles from its northern extremity, while the Appomattox traverses it near its southern borders; on its eastern side it is distant about 13 miles from the city of Richmond; It occupies an elliptical area, the beds lying in a trough, the lowest of them usually highly inclined, where the}^ crop out along the margin of the basin, while the strata higher in the series, which appear in the central part of the basin, are very nearly horizontal. The general strike is about N.N.E. and S.S.W., while that of the nearesr ridges of the Appala- chian chain is about N.E. and S.W. A great portion of these coai measures consists of quartzose sand- stone, and coarse grit, some of the beds, in the lower part of the series resembling granite or syenite, being entirely composed of the detritus of the neighboring granitic and syenitie rocks. Dark carbonaceous shales and clays, occasionally charged with iron ores, abound in the proximity of the coal seams, and numerous impressions of plants, chiefiy ferns and zamites, are met with in shales, together with flattened and prostrate stems of Calamites and Equisetum. These last, how- ever, the Calamites and P^quisetum, are very commonly met with in a vertical position, more or less compressed perpendicularly. That the greater number of Calamites standing erect in the beds above and between the seams or beds of coal, which I saw at points many miles distant from each other, have grown in the places where they are now buried in sand and mud, I entertain no doubt. This fact would imply the gradual accumulation of the coal measures during a slow and re- peated subsidence of the whole region. The coal seams have hitherto been all found at or near the bottom of the series, and the plants in beds below or between them, or immediate- '•' Trans. Ass. Am. Geo. and Nat. t Quar. Jour. Geo. ScL, vol. iii. Mesozoic and Coinozoic Geology and Pala;oniology. 11 ly overlying. One or two species of shells (Posidonomya?) also occur in the same part of the series, at a small height above the coal-seams, and above these a great number of fossil fish, chiefly referable to two nearly allied species of a genus, very distinct from any ichthyolite hitherto discovered elsewhere. Above these fossiliforous beds, which probably never exceed 400 or 500 feet in thicknes!?, a great succes- sion of grits, sandstone and shales of unknown depth occur. They have yielded no coal, nor as yet any organic remains, and no specula- tor has been bold enough to sink a shaft through them, as it is feared that toward the central parts of the basin they might have to pass through 2000 or 2500 feet of sterile measures before reaching the fundamental coal seams. The coal is separated almost everj'where into three distinct beds, and sometimes into five. The upper bed is the thickest, except in a few places where a thin layer of coal is found above it. In some places the main seam of coal is from 30 to 40 feet thick, and at Black- heath it is seen actually to touch the fundamental granite, or is parted from it only by an inch or two of shale. A section at the Midlothian Pit, half a mile south of Blackheath, on the eastern outcrop of the coal, is as follows: Sandstone and shale, 570 feet; slate with calamites, 1^ feet; sandstone and shale, 43 10.12 feet; sandstone with calamites, 8 feet; sandstone and slaty shale, 48 feet; slate and long vegetable seems, 2^ feet; sandstone, 6|^ feet; slate with calamites, h\ feet; sandstone, 14 feet; black rock, 13 feet; slate, 5 feet; main coal, 36 feet; sandstone not laminated, 5 feet; slate, 4 feet; coal, 1 foot; slate, 3 feet; sandstone or grit, 7 feet. Total, 773 10-12 feet. This rests upon granite of unknown depth. Some deduc- tions must be made for the thickness of the beds on account of the in- clination at an angle of 20 degrees. The unevenness of the granite floor is extremel}' great, and the thick- ness of the coal seams quite variable. The disturbances have been extremely great, and dikes of greenstone occur in some places 20 feet in thickness. Some of the upper beds of coal have been reduced to coke, by being deprived of their volatile matter, while others below remain unaltered and bituminous. This is accounted for on the ground that the greenstone, although intrusive, has made its wa}' between the strata like a conformable deposit, and has driven the gaseous matter from the upper coal, while its influence has not extended to lower seams. A remarkable example of coke, in a bed eight feet in thick- ness, occurs at Edge-hill, a locality between five and six miles north of James river, and ten miles north of Blackheath, being on the 12 Mesozoic and Cwnozoic Geology and Paloiontology. eastern outcrop of the basin, and within 500 yards of the granite. The measures passed through above the 8 feet bed of coke, are 110 feet thick, including a conformable bed of blue basalt, 16 feet thick. The shale immediatel}' below the trap is white for 11 feet, and then 25 feet of dark, leafj' shale succeed, below which comes the bed of coke, resting on white shale; and lower down, coal-measures with two seams of inferior coal, each about 4 or 5 feet thick. The shale, 47 feet thick, interposed between the basa't and the coke, exhibits so many polished surfaces or slickeusides, and is so much jointed and cracked, and in some places disturbed and tilted, that we may probably attri- bute the change from coal to coke, not so much to the heating agency of the intrusive basalt, as to its mechanical effect in breaking up the integrity of the beds, and rendering them permeable to water or the gases of decomposing coal. In some places, in the same district, where the upper part of a seam, is coke, the lower is coal, and there is sometimes a gradation from the one to the other, and sometimes a somewhat ab- rupt separation. In the same year, C. J. F. Bunbury* described, from North Carolina, Neuropteris Imna'ifob'n, Pecopteris bullata, FUicites Jimbriatus, and Zamites gramineus. And Prof. Hitchcockf described, from Massa- chusetts, Brontozoum moodi, and B. parallelum. He also discussed the Trap Tuff or Volcanic grit of the Connecticut valley, with the bearing of its history upon the Trap Rock and the Red Sandstone. In 1848, Prof. J. W. DawsonJ describ ;d the New Red Sandstone of Nova Scotia, which extends on the north side of Cobequid bay, from Moose river to the point at the month of North river, and on the south side, from the mouth of Sluibenacadie to the mouth of North river. It rests upon carboniferous strata, and, in some places, presents cliffs rising to an eminence of 400 feet. It is also extensively developed at Blomidon, in the valley of Cornwallis, on the south side of the Bay of Fundy. and at other places. This sandstone appears to have been deposited in an arm of>the sea. somewhat resembling, in its general form, the southern part of the present Bay of Fundy, but rather longer and wider. This ancient bay was bounded by dis- turbed Carboniferous and Silurian strata. The evidences of volcanic action are numerous, and in some places showing great quantities of melted rock brought to the surface, without altering the soft arenace- ous beds through which it has been poured, and whose surface it has ' Quar. Jour. Geo. Soc, vol. iii. t Am. Jour. Sci. and Arts. 2d Ser., vol. iv. t Quar. Jour. Geo. Soc, vol. iv. Mesozoic and Ccenozoic Oeoloyy and Paleontology. 13 overflowed. The Sandstone contains no valuable minerals, and no fossils had then been detected in it. In J 853, Isaac Lea* described, from the Triassic of Lehigh county, Pennsylvania, ('lepsysaurus pennsyloanicns. In 1854, Dr. Joseph Leidyf described, from the Triassic of trince Edward Island, Bathygnathus horealis. In 1855, Prof. J. W. Dawson described Prince Edward Island, which stretches for 125 miles along the northern coast of Nova Scotia and New Brunswick, has everywhere a low, undulating surface, and consists almost entirely of soft red sandstone and arenaceous shale, much resembling the new red of Nova Scotia, and like it having the component particles of the rock united by a calcareous cement. In some places the calcareous matter has been in sufficient abundance to form bands of impure limestone, usually thin and arenaceous. Over the greater part of the island these beds dip at small angles to the northward, with, however, large undulations to the south, which prob- ably cause the same beds to be repeated in the sections on the opposite sides of the island. In the same 3^ear, Dr. E. Hitchcock, jr.;}; described Clathropteris rec- fiusGulus, from the sandstone of Mt, Tom, in Eastharapton, Mass., of the age of the lower Jurassic. In 1856, Prof. E. Emmonsg described, from the Lower Triassic of the Deep and Dan river beds of North Carolina, Chondrites gracilis, C. interruptus, C. ramosus, Gymnocaulus alternatus, Equisetum coliimn- aroides, Dictuocaulus striatus, Itutiodon carolinensis, Clepsysaiirus leai, Palaiosauriis carolinensis, P. sulcatus and Posidonia ovalis, now referred to the genus Estheria, and from the Upper Triassic of the Deep and Dan river beds, Strangeritesobliqitus, Acrostichites oblongus, Pecopteris carolinensis, P. falcata, Pterozamites decussatus, Cyca- dites aciitus, C. longi/olius, Znmites graminioides, Podozamites lanceolatns, P. longifolius, Lepacyclotes circularis, L. ellipticusi Walchia diffusa, W. longi/olia. Catamites disjnnctus, Sphenoglosswn quadrifolium, and Posidonia nialticostata, and P. triangularis, which are now regarded as svnonvms or varieties only of Estheria ovalis. And in 1857|| he described, from North Carolina, Catamites pnnc- tatus, Walchia angustifolia, W. variabilis, W. brevifolia, W. gracilis, Sphenopteris egyptiaca, Cyclopteris obscura. Odontopteris tenaifolia. " Jour. Acad. Nat. Sci., 2d Ser., vol. ii. t Jour. Acad. Nat. Sci., 2d Ser. vol. ii. t Am. Jour. Sci. and Arts, 2d Ser., vol. xx. g N. Carolina Sur. II Am. Geo., pt. 6. u Mesozoic and Ccenozoio Geology and Palwontolof/y. Pterozamites gracilis, P. obtusus, P. linenri-t, P. spatulatns, Dioonites linearis, Stranyerites planus, Pterophyllnm rohustum, Noeggerathia striata, Comcphyllum, cristatum, Arnblypteius ornatus, Rabdiolepis speciosus, Microdns hii'is, Pnhvonornis strnthionoidcs, anil Dromath- c/'«/ miirls, hntC, nia<;iii>Hi,'ui and hlark limostont's, blue and brown shalos and ^^ypsnin. ;M4 IVut in thick- ness. Tiiese meks extend in an inej^jniar belt aeross the State, (Voin the head waters ol' the Hlue and Fancy, across thi« Republican and Solomon, and over the Kansas, betwe(Mj Turkey (JriM'k and the Sal'ne; thonce south and southeasterly up the Smoky Hill and Gypsum, I ol- land and Turkey ('reeks; along the* northern slope of the divi(U', souih of the Kansas, to the iieads of Lyon and Diamond (.'recks; sweeping; thence westward across thc! (/ottonwood and down tlic div'de, soutii of that stream, to tiie Walnut and White Water. Tiie <>ypsnin beds vary in thickness from to r)0 feet, and crop out on the JJluc, the lie- publican, and the Kansas, and on Turkey Creek; and on the divides between the CJypsum and Ilollaiul, and between Turkey Creek and the (Jottonwood. In the same year, Dr. F. V. Hayden* referred the celebrated Pipe- stone quarry of northeastern Dakota, to the Triassic, and showed that the manufacture of it into pipes commenced by the Indians, at a quite recent date — probably witliin the last 'jO or 100 years. The pipestone is called (^atlinite. The Triassic rocks of New Jersey f are included in a belt of country which has the Highland Ranjj;e of mountains on its ncuth- west side, and a line almost straight from Staten Island Sound, near Woodbridge, to Trenton, on its southeast; the Hudson river on the n M'theast, and the Delaware on the southwest. The length of the southern border line is 74 miles; that on the northwest is «i8 miles. These measurements arc from the Delaware river to the State line. Its greatest breadth is on the Delawcre, where it is over 30 miles across. From Mine mountain to the Raritan river, near the mouth of Lawrence Brook, its breadth is 19 miles. On the State line, from the Hudson river to Sufterns, it is 15 miles. The area embraced within these limits, excluding the bays, is about 1500 square miles. Of this about 330 square miles are occupied b}^ trap roclf. It consists of red sandstone, and is fossiliferous, at Pompton, Boonton, Milford, Tumble Station, Belleville, Newark, Pluckamin and other places. The ordinary way of computing the thickness of a rock formation is to take its dip, and also the breadth of country across which this dip is continued, and use them as two parts of a right-angled triangle for- getting the remaining parts, one of which is the perpendicular thick " Am. Jour. Sci. and Arts, 2 ser., vol. xliii. t Geo. ofN. Jersey, 1868. Memtzoir and CUmozoie Qeoloyy and PultfonfoltHfy. 10 npsR of tlio i-ll '■' Proi!. Am. Phil. Soc. t Korr's (Jeo. of N. Carolina, 1875. Emmons 'Jco. Siir. 18."/). M 26 Cincinnati Society of Natural History. I ! ■ clay sliites, shales and conglomerates, generally ferruginous and brick red, but often graj' and drab. The sliales aie occasional!}' marly, and these iiud the sandstones are sometimes saliferous. Many of the beds consist of loose and uncompacted materials, and are therefore easily abraded. The most important and conspicuous member of the series, is a large body of black shales, which enclose scams of bituminous coal 2 to <> feet. This coal lies near the base of the system in both belts, and is underlaid on Dan river by shales; and on Deep river by sandstones and conglomerates; the latter constituting the lowest member of the series, and being in places ver}' coarse. And near the eastern margin in Wake county, where the belt reaches its greatest breadth (some 15 miles), the conglomerates are of great thickness and very coarse, un- compacted and rudely stratified, resembling somewhat the half strati- fied drift of the mountain slopes, the fragments often little worn, and sometimes 10 to 12 inches in diameter, and evidently' derived from the Huronian rocks of the hills to the eastward. The conglomerates of the Dan river belt are among the upper members of the series, and are mostly fine and graduating to grits and sandstones. The black shales near the base of the sj'stem contain beds of fire clay and black band iron ore, interstratified with the coal. They are also highly fossiliferous, especially on Deep river. Silicified trunks of trees are very abundant in the lower sandstones, as may be seen con- spicuously near Germantown, in Stokes county, the public road being in a measure obstructed by the multitude of fragments and entire trunks and projecting stumps (»f a petrified Triasyic forest; and simi- lar petrifactions are abundant in the Deep river belt, occurring in this, as in the other, among the sandstones near the horizon of the coal. The actual vertical depth to the underlying Archrean rocks on Dan river may not exceed 1000 feet, but what was the original thickness of the strata before denudation began can only be conjectured. The beds on Dan river, however, measured at right angles to the dip, gives a minimum thickness for that side of the formation of near 10,000 feet. In the section of the Deep river belt, which is exposed in the valley of the Yadkin, not onl}' is there a width of six miles with the usual dip of 20°, but there is an additional outcrop more than a mile in breadth, ten miles south of the principal belt, which preserves the southeasterly dip of nearly 20°, and Jience the calculation for a minimum thickness, at this margin, must be based on a breadth of 16 miles, which gives a thickness of more than 25,000 feet. There is no way of accounting for the present position of these beds Mfisozoic and Cwnozoic Geolor/if and Pala'ontolof/jj. 21 with their opposite and considerable dips, but by supposing an uplift of the intervening tract, such and so great, that if the movement were now reversed, it vvould carry tliis swell of nearly 100 miles breadth into a depression much below tlie present level of the troughs in which these remnant fringes lie, so that there has been an erosion not only of 10,000 to '2{),000 feet of the broken arch of Trias^sic beds over this area but also of a corsiderable thickness of the underlying rocks on which they had been deposited. The present area of Triassic in North Carolina is about 1,000 square miles, about one third of which, it is estimated, is underlaid with coal. Prof G. K. Gilbert* found a section of the Trias exposed by the North fork of Virgin river, from the vicinity of Mountain Lakelet to Rockville, in Southern Utah, ',],2M) feet in thickness, and the Jurassic at the same place :?50 feet. Tlie Triassic on tlie West Fork of Paria ^ Creek, 2.575 foet, and the Jurassic 740 feet. And the Triassic at Jacob's Pool, Northern Arizona, 2,150 feet in thickness. E. E. Ho- well estimated the Trias at Rock Canon, near Provo in the Wahsatch Range, at from 4,000 to 5,000 feet, and the Jurassic from 6,000 to 8,000 feet. On Pine Mountain, the Trias at 4,050 feet, and the Jurassic at 1,200 feet. On the Dirty Devil river in Northern Utah, the Jurassic is about 800 feet thick, on the southwest side of Escalante river, 60 miles far- ther south, from 1,000 to 1,200 feet. The thickness of the Triassic in New Mexico and Eastern Arizona is from 1,200 to 1,800 feet. This gradually increases to the westward until near Paria, it is 2,250 feet Ninety miles to the northeast, on the Dirtj^ Devil river, 1,700 to 1,900 feet, is found, while near St. George, farther west, the thickness is esti- mated between 5,000 and 6,000 feet. J. J. Stevenson found the Triassic on Beaver Creek, a few miles northeast of Canon City, 2,700 feet in thickness, and unconformable with the Jurassic above, wherever it is observed in this region. Prof. G. M. Dawson, f separated the Triassic or Jurassic of the Rocky Mountains, near the boundary' monument, in descending order, into — 1st. Fawn-colored flaggy beds, 100 feet. 2d. Beds characterized by a predominant red color, and chiefly red sandstone, but including some thin greyish beds, and magnesian sandstones, the whole generally thin bedded, though sometimes rather massive. Ripple marks, etc., weath- ers to a steep rocky talus, where exposed on the mountain sides ; and passes gradually down into the next series, 300 feet. 1^'^ i' '•" Geo. Sur. W. 100th Meridian, vol . 3. t Rep. (leo, 49tli Parallel. ^ii 28 Ciaohinatl Society of Katural History. 1 1 Theo. B. ('oinstoc'k* found the Jurassic liincstoncs outcroppin' of the Triassie (rroup of Colorado and the Went, as late as 1870, says: The Red Beds or Triassie Group is very persistent, and if absent at all, only at very short intervals. No organic remains have yet beea found in this group, l>y the meinlKjrs of the survey under my charge, yet, for various reasons, we have assumed the red sandstones to be of Triassie Age. It is barely possible that a [)ortion or all of the Group is of Jurassic Age. Yet Prof. Cope is of the opinion that he has dis- covered evidence in New Mexico of its Triassie Age. The history of this Group is still obscure, and remains as one of the problems to be solved by more extended and more thorough explorations. Geograph- ically it is one of the most widely distributed formations in the west. From the northern boundary to the southern line and east of the Wa- satch range, in Utah, this red formation makes its appearance wherever a mountain range is elevated so as to expose the various sedimentary groups. The evidence indicates that it extends without an}' import- ant interruption over the broad area as defined above. These red sandstones have alwa3's attracted much attention, on account of their peculiar color, but nowhere have lever observed them performii.g such a conspicuous part in giving form to the scenery of the country, as along the eastern base of the Rocky Mountains in Colorado. This feature is more marked from a point about fifty miles north of Denver to Colorado Springs, than in any other portion of the continent. Along this belt the sandstones are more compact, with every variety of red, from a pale, dull tint to a deep purple color. There is also every variety of texture, from a rather coarse conglomerate to a fine sand- stone. It\ariesmuch in thickness, ranging from 400 to 2,000 feet. These sandstones in Pleasant Park, the '• Garden of the Gods," and other places have been weathered into the most fantastic shapes, and stand up in immense walls or columns from 5U to 250 feet in height. Dr. A. C. Peale found Permian fossils in the beds below the red sandstones referred to the Triassie, and as Dr. Hayden and others had * Carroll to Yellow Stone, Nat. Park, t U. S. Geo. Sur. Terr McHozoic and Ccsnozofc Geology and Palmontology. :u Cound Juiussic foHsils, in the beds above, which are referiod to Juras- sic age, it left tiie conclusion with him that the reu sant]stones are of Triassic age. The credit, liowever, of lirst announcing the age of these sandstones is due to JNI. Jules Marcou, who, as early as 185:1, in his "geological map," etc., "with an ex|)lanatory t(!xt, " referred the beds of conglomerate, described by ('ai)t. Stansbury, in the environs of th(! Devil's Gate, Rocky Mountains, and the conglomerate and sand- stone described by Prof. Dana, on the Shaste river, and the boundary between Oregon and California, to the Trias. I'he reader may also be referred to his " Resume and Field Notes," in Vol. 3, Pacific R. R. Sur- ve}', where he identified these rocks at numerous places near the Uuth parallel. Dr. Pealc found a section of Jurassic rocks, at the head of Second Canon, Eagle river, about *.)40 feet in thickness, and consisting of marls, sandstones and limestones. Another on Roaring Fork below station No. 14, -14:0 feet thick, and another in the lower Canon of Gun- nison river, near station GO, representing 212 feet in thickness. It oc- curs usually only as a narrow belt outcropi)ing beneath the Dakota Group. In 1877, Arnold Hague* estimated the thickness of the Triassic on the outlying ridges and foot h'lls of the east side of the Colorado Range at 800 feet. The group is found immcdiatel}' overlying the Coal Measures all along the foot-hills of the range, the continuity of the out crop being broken in on!}- a few places, and in most cases, simply by being concealed below the uncomforraable Tertiary beds. The rocks are characterized by a prevailing brilliant red color, which shades oft' into yellowish and whitish tints, and, near the top and bot- tom of the series, show frequently reddish-gray bands. The deep brick- red color, however, is so persistent as to form one of the most clearlj-- defined geological horizons of the uplifted sedimentary beds. The group reaches its greatest development to the southward in Colorado, between the Big Thompson and Cache la Poudre, while north of the railroad it appears much thinner, and, between Lodge Pole and Horse Creek, reaches its minimum. Still farther to the northward, in the region of the Chugwator, it again thickens, but scarcely attains the thickness in Colorado. A section atChugwater shows between 500 and 600 feet of strata, and another at Box Elder Creek, G50 feet. Sandstones form by far the greater part of the eutire series of strata. Even the conglomerates, shales, clays and earth}' beds, which occur in- * Geo. Expl. 40th Parallel. •.\2 Cincinnuti Society of NntHrnl lUsfory. V\P >i ;?i:i torst rati Hod, nppoarnioroorloHfiaronacoojiH, nnd nro really closely allied to true HandHtones, only sliowiiij^ coiisidenilile diversity in texture and ineehanieal eondltions. Deponits of gypstiun are very eoinuiou in the upper bedn. The TrinHsic is exposed aloiiji; the Laramie river, exhihitinif a series of nearly horizontal strata, 1,0(10 feet in thiekness. In one plaec a de- posit of pure solid ij;y|)siini, 22 feet in thiekness, oeeiirs, lyinf>' between two l)eds of hard red sandstone. In the North Park the thiekness is (stiniatcd at lOCO ftiet. S. F. Emmons * found tiie Triassie in the vicinity of Rawlinjif's Peak, 000 feet in thickness. And in the Uinta Mountains, from ;i.700 to 4,000 feet. At its base is a series of clayey beds, havinj? a thickness of 1,200 to 1,500 feet, abont eciually divided by a thin bnt persistent bed of limestone. This is succeeded b}- the Red IJed Group in a thickness of about 2,500 feet, princii)ally of sandstones. In Henry's Fork Basin, which is a narrow valley, extending 15 miles in either direction, cast and west from Crreen river, with a width of about n miles, and whose average level is about 300 feet below the cen- ter of the Bridger Basin proi)er, the Triassie sandstones in Flaming Gorge Ridge, near Green river, are exposed in perpendicular cliffs, about 1,200 feet i'l height, while having at their base an undetermined thick- ness of clay beds. In Emigration, Parley and Weber Canons, in Utah, the Triassie is exposed from 800 to 1,000 feet in thickness. Tlie Jurassic is also present, and in some places has an estimated thickness of 1,500 to 1,800 feet. The Triassie, in the Desatoya and New Pass Mountains of Nevada, contains highly fossiliferous calcareous shales and limestones. In the Pah-Ute Range in the region of Dun Glen Pass, fossils indicating Ju- rassic and Triassie ages are found associated together. The Triassie is represented in the West Humboldt Range, Nevada, in Cottonwood, Buona Vista, Coyote, Bloody and 'Star Canons. Single sections expose strata 1,500 feet or more in thiekness. Arnold Hague* estimated the thickness of the Jurassic on the out- lying ridges and foot hills of the Colorado range at 250 feet, down to 50 feet and less. The rocks consist of loose friable sandstones, lime- stones, marls, and impure clays, presenting great variety in color and texture, and passing from one to the other by almost imperceptible * Goo. Sur. 40th Parallel. Mesozoic, ami Cnnozoic (icolnyy and Pala:onfolo()ij. :{3 grados. The lino Hcpanitinj? this jj^roiip from th« Tiinssif is not I'li'iirly (ledncd, iiiid tlio scpiinitidii tluTororo is soint'wimt arliitriiry. 'I'lu' ^I'oiij) iittiiins its gr»'iiU'st tliickiu'ss in tlu! n'^ion ol'llij^ Tlioinp- son ( 'rt'i'Iv, in (\)1'M'ii(1(). Iti \Vy(nnln,u;, ulonj^ Lodge I'olc and Il(trsi) Creeks, it is re|)i'i'«ente(l by only iilxMit 7'» feet of stnita. Still riirtlier to tlio northward it o::j)ands ji^ain to a thieknt'ss of !.')() feet. On the Laramie Plains west of Antelope (Jreek the thiekness is estimated at 200 feet. On Como Uid^e, in the (ixtreme n(nth\vestern corner of the Laramie Plains, Just west of the lOOth Meriilian, the Jurassic rocks exhibit all the characteristic; strata that have hi'cn observed in other localities, associated with orj^anic remains, and possessing a thickness of from 17^) to 200 feet. Its thickness in the North I'ark is estimated at from 200 to 250 feet. S. F. P2mmons* estimated the average thickness of the Jurassic in the Uinta Mountain Region at from 000 to 800 feet, in which the lime- stones are highly fossil iferous, and have a thickness of 200 or '.iOO feet, the remainder being made up of sandstones, shales anil clay beds, re- markable, where well exposed, for their bright, variegated colors. In Henry's Fork Basin, a Ihiikness of IJOO to 400 feet is observed in the elitt's overlooking Sheep Creek. In the Montezuma Range, Nevada, the shales have a thickness of between 3,000 and 4,000 feet, and rest directly upon granite. North of Indian Pass, and at Antelope Peak, they reach a development of 4,000 feet. F. B. ]Meekf described, from the Triassic at Buena Vista Canon, Nevada, Sphcura whitneyl, Modwniorpha ovata, Jlodioviorpha lata, Gymnotoceras rotelliforme, Arcestfis peiplamis, A. (jahbi, Acrochordi- ceras hyatti, Entomoceras laithei, Eudiscoceras yubbi. Hall and Whitfield, from the Trias ofPah-Ute Range, Nevada, Spirifera alia, Kdmondia myrlna. Prof. E. D. Cope,]; from the Trias at Phoenixville, Pa., Palaeocfonus appalachianus, a gigantic carnivorous dinosaurian, F. anlacodus, now Suchoprion aulacodus, Clepsysaunis veatleianun, Suchoprion cypho- don, Thecodonlosaurus g ibbidens ^^ and Palaeosaurnsjrazeranus^ from Texas, Eryops meyacephalus; and from Painted Canon, in Southeast- ern Utah,! Dystrophaeus vioemala;. I ■?.! I ■! I ■ - Gflo. Sur. 40th Parallel. t U. S. Geo. Expl., 40th Parallel, vol. 4. t Pal. Bull.. No. 26. § Proc. Am. Phil. Soc. 1 Wheeler's Sur. W. lOPth Mor., vol 4. 34 Cincinnati Society of Natural History. ilf % ;'l:i r! ;' f ^^^ Prof. C. A. Wliito,* from the Jurassic south of Dirty Devil river, Utah, Ostrea strigilecula; from the North Fork of Virgin river, Ino- cerainus crassalatus ; and from Camp Cottonwood, Old Mormon Road, Nevada, Myophoria, amhilinenta. F. B. 3reok,f from the Jurassic at New Pass, Desatoya Mountains, Nevada, Limn erecta; from the Weber (!anon, Wasatch Range, Pinna kinyi, Cucidloia hagnei, Jfyacites inconspicuns^ 3fyacites iceberensis^ and from Cottonwood Canon, Belemnit.es nevadaensis. Hall and Whit- field, from the Jurassic at Flaming Gorge, Uinta Range, Utah, lihyn- chonella myrina, Limn occidentalis, from Chalk Creek, Astnrte arenosa, from Shoshone Springs, Augusta Mountains, Nevada, Terehratula angicsta, Aviculopecten aufjustcnsis, Septocardia typica^ S. carditoidea, from Wyoming Natica lelia, Gamptonectes pertenuistriatus, Trigonia quadrangularis\ Prof E, D. Cope first suggested that the rocks at Canyon City, Colorado, supposed by Prof Hayden to belong to the Dakota Group (and also those in the same horizon, 100 miles north, supposed b^- Prof iNIarsh to be lower Cretaceous), are Jurassic, and described]; Cam- arasaurus stipremns, Compsemys plicatuUis,^ Caulodon diversidens, Tichosteus lucasanus, Atnphicailias alf.i(s,\\ A. latus, Symphyrophus miisGidosns,^ Caulodon leptognmun, Lailaps triJiedrodon.** And Prof O. C. Marshf f described, from the Upper Jurassic rocks on the eastern flank of the Rocky Mountains, Stegosanrus armatus, Atlantosanrns montanus, Apatosaurus ajax, A. grandis, Allosaurus /ragilis, Nanosaurus rex. In 1878, J. F. Whiteaves];J pointed out the Jurassic Age of certain rocks exposed on Iltasyouco river, in British Columbia, and described Pinna suhcancellata. Grammatodon Utasyoucoensis and Trigonia dawson i. Prof E. D. Cope, from near Canyon City, Colorado,§§ Hypsirophus discurus, Brachyrophus altarkansanus, Amphicotylus lucasi, Tichos- tens a-quifacies, and Sphanterias a7nplexus.\\\\ Prof O. C. Marshf ^ described, from the Upper Jurassic of Colo- rado, Atlantosnurus immanis, Jlorosanrits impur, Allosaurus lucaris. <* Wheeler's Sur. W. 100th Mer., vol. 4. t U. S. Geo. Expl. 40th Pfirallel. t Pal. Bui., No. 25. g /Wrf.,No. 26. || * • Bull. U S. Geo. Sur. Terr., No. 3. tt Am. Juur. Sei - occasional beds of water- rounded detritus, which he regarded as of Triassic Age. Dr. C. A. White described,! from the Jurassic of southeastern Idaho, Terebratula semfsim/dex, Avicnlopecten pealei, A. altus, 3Iee/coceras aplanatum, 31. gracilitatis, 31. mushhachanum, and Arcestes cirratus. Prof O. C. Marsh;]; described, from the Jurassic of the Rocky ]Moun- tains, Stylncodon gracilis, Ctenacodon serratus. Dryolestes arcuatus, Tinodon robustus, T. lepidvs, Brontosmirus excelsus, camptonotus ampins, C. dispar, Coehwus frag His, and Stegosaurus ungulatus. And Prof E. D. Cope§ described, from the Jurassic of Colorado, Caynarasaurus leptodirus and Hypsirhopiis seeleyanus. Jurassic strata were determined at Cook's Inlet, in Alaska, as early as 1848. and Grewingk described,! from this place, Ammonites tvos- nessenski, and identified A., hiplsx, Belemnitella paxillosa, and Utiio liasinus. And in 1857, Jurassic strata were determined at Point Wilkie on Prince Patrick Land, far north of British America. It was from this place that Capt. McClintock collected the fossils described by Prof Haughton^ as Ammonites macclintocki and 3fonotis (Avicula) septentrionalis. In taking a general view of the Triassic and Jurassic strata, we see them in the eastern part of the continent consisting of narrow belts, having an immense thickness. The thickness in the Connecticut Val- ley is but little short of four miles, while in New Jersey it exceeds five miles. Israel C. Russell has argued that th'^ ph3^sical history of these beds, in New Jersey and Connecticut, tends strongly to show that the two areas are the borders of one great estuary deposit, the central por- tion of which was slowly upheaved, and then removed by denudation. That the trap sheets were derived from a reservoir beneath the estuary deposits, and represent in part the force that caused the upheaval. The outburst of trap must have been the closing event of the Triassic changes, and have occurred after the sedimentary beds had been up- ^1 I •hi It ' ■■■• Geo. Sur. Can. t BuU. U. S. Sur.. Vol. 5, No. 1. X Am. Jour. Sei. & Arts, 3d sor.. vol. 18. ^ Am. Nat., vol. 13. llVerhandlungen dor Russisch-Kniserliehen mineralogischen Gesellschaft zuSt. Petersbourg. If Jour. Roy. Dub. Soc, Ireland, v 36 Cincinnati Society of Natural History. I ir m beavccl and eroded. And that the detached areas, even to North Caro- lina, must have been pai't of the same estuary formation, now broken up and separated through the agency of upheaval and denudation. Much denudation has evidently taken place, which must be added to the enormous thickness which still exists to ascertain the original dimensions of the deposit. All this points to a great depth of the sea, or the ba3's, as the case may have been, in which the deposits were made. But when we turn to the Triassic and the Jurassic of the West, we observe them extending from Mexico far into British Columbia, and covering hundreds of thousands of square miles. Over extended areas the Triassic is more than a mile in thickness, and superimposed upon it is a great thickness of the Jurassic ; and again the Jurassic is found more than a mile in thickness resting upon the heavy-bedded Triassic strata. The maximum thickness, therefore, of these forma- tions over great tracts of'country is more than two miles, and the ques- tions very naturally arise, what age do they represent ? Could the deposits have been rapidl}' made, and therefore represe.it only a brief space of time, or were they extremely slow and indicative of the lapse of millions of years? Were the deposits made in shallow water, or in the depths of mid-ocean? Is there a deposit now taking place that bears any resemblance to these, and if so, what light if any does it throw upon the subject? And what does palreontolog}-, the criterion by which all rooks are to be judged, offer to enligliten us in regard to the secrets of this vast accumulation of detrital material? All deep-sea dredgings have shown, that at great depths in the At- lantic and Pacific Oceans, there is a deposit of red mud constantly taking place. We think it bears some resemblance to the red sand- stone of the Triassic and Jurassic periods, and in order that a com- parison may the more readily be made, we quote from the mo i^ mc- cessfulof the many exploring and deep-sea dredging expedition Sir C. Wy ville Thomson says,* speaking of the first time thai th** dredge brought up the mud from the bottom of the Atlantic at the depth of 3,600 fathoms: "This haul interested us greatly. It was the deepest by several hundred fathoms which had yet been taken, and, at all event? coinci- dently with this great increase in depth, the material of the bottom was totally different from what we had been in the habit of meeting with in the depths of the Atlantic. For a few soundings past, the ooze had been assuming a darker tint, and showed on analysis a continually lessening •■' Voyage of the Challenger, vol. 1, 1878. s ■' Mesozoic and Ccnnozoic Geology and Paloiontology. 37 amount of calcareous matter, and, under the microsco))e, a smaller num- ber of foraminifera. Now calcareous shells of foraminifera were entirely wanting, and the only organisms which could be detected, after wash- ing over and sifting the whole of the mud with the greatest care, were three or four tests of foraminifera of the cristellarian series, made up apparently of particles of the same red mud. The shells and spines of surface animals were almost entirely wanting; and this is the more remarkable, as the clay-mud was excessively fine, remaining for days suspended in the water, looking in color and consistence exactly like chocolate, indicating therefore an almost total absence of movement in the water of the sea where it is being deposited. When at length it settles, it forms a perfectly smooth red-brown paste, without the least feeling of grittiness between the fingers, as if it had been levigated with extreme care for a process in some refined art. On analysis it is almost pure clay, a silicate of alumina and the sesquioxide of iron, with a small quantity of manganese." After a great deal of experience in sea dredging, he says: "According to our present experience, the globigerina ooze is limited in the open oceans — such as the Atlantic, the Southern sea, and the Pacific — to water of a certain depth, the extreme limit of the pure characteristic lormation being placed at a depth of somewhere about 2,250 fathoms. " Crossing from these shallower regions occupied b}' the ooze into deeper soundings, we find universally that the calcareous formation gradually passes into, and is finally replaced by an extremely fine pure clay, which occupies, speaking geuerallj', all depths below 2,500 fathoms, and consists almost entirely of a silicate of the red oxide of iron and alumina. The clay is often mixed with other inorganic mat- ter, particularly with partif'les, graduating up to the size of large nod- ules, of peroxide of manganese; and in volcanic regions, or in their neighborhood, with fragments of pumice. The transition is very slow, and extends over several hundred fathoms of increasing depth; the shells gradually lose their sharpness of outline, assume a kind of ' rot- ten' look and a brownish color, and become more and more mixed with a fine amorphous red-brown powder, which increases steadil}'- in pro- portion until the lime has almost entirely disappeared. This brown matter is in the finest possible state of subdivision, so fine that when, after sifting it to separate any organisms it might contain, we put it into jars to settle it remained for days in suspension. " We recognize the gray ooze as, in most cases, an intermediate stage between the globigerina ooze and the red clay; we find that on one I '■ill 88 Cincinnati Society of Natural History. .'I II: side, as it were, of an ideal lino, the red clay contains more and more of the material of the calcareons ooze, while on the other the ooze is mixed with an increasing proportion of red cla}-. " From Teneriffe to Sombrero, the depth goes on increasing to a dis- tance of 1,150 miles from Teneriffe, when it reaches 3,150 IVitlioms ; there the clay is pure and smooth, and contains scarcely a trace of lime. From this great depth the bottom gradually rises; and with de- creasing depth the gray color and the calcareous composition of the ooze retui'n. Three soundings in 2,050, 1,900, and 1,950 fathoms, on the ' Dolphin Rise,' gave higlily characteristic examples of the (jlo- bir/erina formation. Passing from the middle plateau of the Atlantic into the western trough, with depths a little over 3,000 fathoms, the red clay returned in all its purity; and our last sounding, in 1,420 fathoms, before reaching Sombrero, restored the globigerina ooze with its peculiar associated fauna. "The distance from Teneriffe to Sombrero is about 2,700 miles. Proceeding from east to west, we have about 80 miles of volcanic mud and sand ; 350 miles of globigerina ooze; 1,050 miles of red clay; and 330 miles of globigerina ooze; 850 miles of red c\i.y\ and 40 miles of globigerina ooze, giving a total of 1,900 miles of red clay to 720 miles of globigerina ooze. "The nature and origin of this vast deposit of clay is a question of the very greatest interest; and although I think there can be no doubt that it is in the main solved, yet some matters of detail are still iuA'olved in difficult}'. My first impression was, that it might be the most minutel}' divided material, the ultimate sediment, produced by the disintegration of the land b}' rivers, and by the action of the sea on exposed coasts, and held in suspension and distributed b}' ocean cur- rents, and onl}' making itself manifest in places unoccupied by the globigerina ooze. Several circumstances seemed, however, to negative this mode of origin. The formation seemed too uniform; whenever we met with it, it had the same character, and it only varied in composi- tion in containing less or more carbonate of lime. "Again, we were gradually becoming more and more convinced that all the important elements of the globigerina ooze lived on the surface; and it seemed evident that, ho long as the conditions on the surface remained the same, no alteration of contour at the bottom could pos- sibly' prevent its accumulation; and the surface conditions in the Mid- Atlantic were very uniform, a moderate surface current of a very equal temperature passing continuousl}'^ over elevations and depressions, and everywhere yielding to the tow-net the ooze-forming foraminifera Mesozoic and CUvnozoic Geology and Falceontoloyy. :i\) in tlio same proportion. The Mid-Atlantic swarms with pelagic mol- lusca; and in moderate depths, the shells of these are constantly mixed with the globigerina ooze, sometimes in nnmber suflicient to make np a considerable portion ol' its bulk. It is clea'" that these shells must fall in equal numbers upon the red clay; but scarceh' a trace of one of them is ever brought up by the dredge on the red clay area. It might be possible ta explain the absence of shell-secreting animals liciny on the bottom by the supposition that the nature of the deposit was in- jurious to them; but the idea of a current sufllciently strong to sweep them away, if falling from the surface, is negatived by the extreme fineness of the sediment which is being laid down. The absence of surface shells appears to be intelligible only on the supposition that they are in some wa}' removed by chemical action. "We conclude, therefore, that the red cla}' is not an additional sub- stance introduced from without, and occupying certain depressed re- gions on account of some law regulating its deposition; but that it is produced by the removal, by some means or other, over these areas, of the carbonate of lime, whicli forms probabl}' about 98 per cent, of the material of the globigerina ooze. We can trace, indeed, e\c'vy succes- sive stage in the removal of the carbonate of lime, in descending the slope of the ridge or plateau where the globigerina ooze is forming, to the region of the clay; we find, first, that the shells of pteropods and otiicr moUusca, which are constanth' falling on the bottom, are absent; or, if a few remain, thej' are brittle and yellow, and evidently decaying rapidly. These shells of mollusca decompose more easily', and disap- pear sooner than the smaller, and apparently more delicate shells of rhizopods. The smaller foraminifera now give wa}', and are found in lessening proportion to the larger; the coccoliths first lose their thin outer border and then disappear; and the clubs of the rhabdoliths get worn out of shape, and are last seen, under a high power, as minute cylinders scattered over the field. The larger foraminifera are at- tacked, and instead of being vividly white and delicatelj' sculptured, they become brown and worn, and finally they break up, each accord- ing to its fashion: the chamber-walls of (?Zo6<(/er«/ia fall into wedge- shaped pieces, Avhich quickl}- disappear; and a thick rough crust breaks awa}- from the surface of Orhulina, leaving a thin inner sphere, at first beautifully transparent, but soon becoming opaque and crumb- ling awa}'. " In the mean time, the proportion of the amorphous, red cla}' to the calcareous elements of all kinds increases, until the latter disappear, with the exception of a few scattered shells of the larger foraminifera, 40 Cincinnati Society of Natural History. f ^s ;:( ; t V J .ontolofjy. 11 tho (loop depressions, the eastern, tlie northwestern, and the south- western basins. An intornjediate band of gray ooze occurs in the Atlantic at depths averaging [)erhaps from 2,100 to 2,;{00 Cathonis. " Over the redehiy area, as niiglit have l)ecn e\'pe('ted IVoin the mode of formation of tiio red clay, th(! pieces of pumice and tlie re- cogniiiabhi mineral fragments were found iu greater abundance; for there deposition talces place much more slowly, and foreign bodies are less readily overwhelmed and masked; so abundant are such fragments in some places, that the fine amori)hous matter, which may be regarded as the ultimate and universal basis of the deposit, a[)pcars to be present only in small proportion. "The clay which co\'ers, l)roadly speaking, the bottom of the sea at depths greater than 2,000 fathoms, Mr. IMurray considers to be pro- duced, as we know most other clays to be, by the decomposition of feldspathic minerals; and 1 now believe that he is in the main right. I can not, however, doubt that were pumice and other volcanic pro- ducts entirely al)sent, there would still be an impalpable rain over the ocean-floor of the mineral matter, which we know must be set free, and must enter into more stable combinations, through the decomposition of the multitudes of organized beings which swarm in the successive layers of the sea; and I am still inclined to refer to this source a great part of the molecular matter which always forms a considerable part of a red- clay microscopic preparation." It is quite clear, that it would require millions of years for an ac- cumulation to take place two miles in thickness, at the progress now in operation in the Atlantic, at depths from three to five miles. And one can not help thinking that such deposits bear strong resemblance to the red sandstones of the Jurassic and Triassic str.ita, and conclud- ing, unless there is some reason to be drawn from other sources, to in- fer a more rapid deposition in the formation of the latter strata than that which prevails at the present time, that one is the representative of the other as to the depth of the ocean and the material and method of the deposit. If this be so, the Triassic and Jurassic rocks represent an age of vastly greater duration than the combined Cretaceous, Tertiar}' and Post-pliocene periods. Palaeontology may not follow such a comparison all the way to the final conclusion, but it walks hand in hand so far that we are at a loss to imagine where the separation maj' be made. There are many classes and orders of animals that never find a tomb in the great depths of the Atlantic, there are others that start for that goal but reach it only iu the shape of an impalpable powder, "the insoluble ■?. ,' ' ■; 42 C incinnati Society of Natural History. M \ \m \'^ im residue, the anh as it were of the ealcarooiis organisms." And as to the rest they are sparsely distributed. In tliis resi)ect the comparison witli the Ti'iassic and Jurassie is most favorable, as the rarity of fos- sils in the hands of tho collectors very clearly testifies. But when we examine the fossils that have been discovci'cd, and note the evolution of forms, and compare these with tlie progress in other ages, we are most profoundly impressed witli the immense lapse of time that must bo ascribed to these periods. As not a single species that is found in rocks earlier than tiio Triassic, and not one that is found in rocks more recent than the Jurassic, has ever been found in either the Triassic or Jurassic strata, we are sen* at once to tlio genera for comparison. Let us first turn to the Vegetable Kingdom. It is represented in the Triassic and Jurassic of North America by 66 described species, distributed amouf 30 genera. Twelve of these genera are also of pahieozoic age, viz.: Cnhnnites, Chomlrites, Cyclop- teris, Dadoxylou, Fucoides, JSTeuropleris.^ Noeyyerathia, Odonfopteris, Pecopteris^ Sphenoptcris^ Taniiopteris, and Walchia ; and seven genera are found in the Cretaceous, or more recent strata, viz.: Chon- drites, Eqnisetum, Neuropteris, Pecopteris, Pterophyllum, Sphenop- teris and Tmniopteris. This shows that five genera only, or one sixth of all that are known, passed through this period, aiul that during this period 10 genera, or more thai* hidf of what ?re known, came into ex- istence, and also became extinct. The chanjio of forms, as thus indi- cated, is greater than that which has occurred to the Cretaceous flora during all the ages that have elapsed to the present time. The evidence furnished by the invertebrate kingdom is no less strik- ing- Thus far no species belonging to the Annelida or Crustacea, has been described from these rocks, and the onl}' articulated animal- found fossil, so far us T have ascertained, is the 3Iormolucoides arti- culatus, described by Prof. Hitchcock, in 1858, — a genus unknown in other rocks. The class Pteropoda and the Rudista are unknown. The class Polypi is not represented b}' a described species, and the Cavea prisca alone represents the Br3'ozoa — another genus unknown in other rocks. The Echinodermata is represented by an Asterias and a Pentacii' nus, genera unknown in the Pala30zoic age, but one of them passed up into the Cretaceous, and the other into the Tertiary period. The Brachiopoda are represented b\' eleven species belonging to the genera Linyida, lihynchonelln, Spirifera and Terebratula. All of these are Palicozoic genera, and all of them have continued an exis- 3Iesozoic and ('cBiiozoic Gcolof/if and PaUvontolorfi/. 13 tcnce to recent times, except Spirifera, wlilcli, so fjir as known, ternii- natcil its career in the Jurassic aj^e. Tile Gasteroi)o(la is represented by nine species belonyinj^ to eiglit genera. Two of tiiesc generr Dentaliton and Turho, had an existenco, in tlie Palreozoic age, and continued to live until tlie Tertiary period. One genus Lu)placodt;s von\n\Q,nQO<\ aui\ tenniiiated during the age in question. The other five g(!nera, JVcrilc/ld^ XcrUind, Plnnorbis, V, lielemnites and Ceratitcs, commenced t'eir existence in the age in (question, and terminated their career in the Cretaceous period. The Lamellibranchiata is repi'csented by 125 species distributed among ol genera. Six genera, Avicuht, Cardium, Lima, Jfijfi/uf}, Os- trea and Pinna, arc reckoned among tlie paheozoic and living. Of the other 45 genera, eleven of them are pahtiozoic, but only 24 have yet been found in the Cretaceous. 1*.) of these are Tertiary, and 7 are living, all of which are marine except Unio, which is now a fresh-water genus. Or looking at this most numerously represented class of the Inverte- brata in another light, wo observe that of the 51 genera represented in the rocks in question, 13 genera, or more than 25 per cent., are still liv- ing. 21 genera had passed awa3' before the Cretaceous period, leaving 30 genera only in the latter period; and consequentl}' only 17 of these genera have expired since the dawn of the Cretaceous. The vast changes in the vertebrate kingdom during this period, and the grand passage from the Batrachla to the iMammalia, evidences the same great laspe of time that is indicated b}'^ other organic remain, and Inferred from the vast thickness and extensive distribution of the strata. The class Pisces is represented by fifteen species belonging to nine genera. Two of these genera, Ambhjpterus and Pnlmoniscus, are also of PalfEozoic age. The other seven are not represented so far as known in rocks of older or younger age. The class Aves is represented only hy Palaeonornis struthionoides, a bird named by Prof. Emmons, in 1857 — a genus, however, not 3'et clearly defined or understood. The class Reptilia is represented by 41 genera, nona of which are of PfJffiozoic age, and only two, Ladaps and Pterodactylus, are said to 44 Gincinnnti Society of uVatural His fori/. :.i'l reuc'li the Crfitaccons era. Wlierc tracks hiive been (loscrihod now genera in all iiistanr(>s have; Ix'cn [)i'()po.s('(l. Tlu! "^raniinalia are reiJieseiiteil in tiie Triassic nn-kn by I)fo)ntifh<;- riiDH nflccsfrc, dc^snibed by I'rof. Emmons, in 18r>7. Vouv j^cnera have been named IVoin the Jurassie, viz: (Jtenacodov^ Drtjolcstcs, Styldcodoi) and Tinodon. These {genera are not only eonllned to the roeks in question, but they are not releired to fanuliea found in other rocks. Or taken as a whole, the vertebrate kin_«>-dom is represented by hi genera, two of whieh only are referred to rocks of earlier (bite, and only two to a later periocb These calculations are based ui)on our present knowleilge of the fauna and flora, but as new discoveries are being made almost (biily, we can not tell how much thej- may be modified in future. It will be observed, however, that an increased number of species will not change the calculations, and that an increase of the genera is more likely b^' adding new ones, than b}' the discovery of either Palncozoic or Creta- ceous genera in these rocks. Amphicadlas frcif/illimus was described by Prof. Cope, from near Canyon City, Colorado, in 1878, (See Am. Nat. for August.) Ilypsir- hopus secleyanus should have been referred to the Jurassic of W^'om- ing, instead of Colorado; and Palccoctonas ((ppalachiantis, Suchoprion (luliicodus, C'lepsyscan'us ceatlciauHs, Suchopvion cyphodott, Thecodon- tosaai'Hs gibbidcns, and PaheosaKVus frazeranus should have been re- ferred to York County, Pennsylvania, instead of Phoenixville. We will now pass the Triassic and Jurassic periods for the purpose of considering the Cretaceous or last period that is referred to Mesozoic age. v^ RETACEOUS. \i The existence of the Cretacoous formation, upon this continent, was lirst determined in the year 1827, when Dr. S. G. Morton and Lardner Vanuxem* compared the marl of New Jersey with the Cretaceous of Europe, called by the French la craie inftrieure on aucienne, and by the English the Green wSand formation or Ferruginous Sund-serles. In 1828, Dr. J. E. DeKayf described, from New Jersc}^, Ammonites hippocrepis, now Scaphites hii^pocrepis., and A. 2)lacenta^ now Placen- ticerus placenta. [To BE Continued.] * Am. Jour. Sci. & Arts, vol, 12. t Ann. Lye. Nat. Hist., N. Y., vol. 2. McHOZoic (intl (Ja'tiozoit; frenhxiji miil Pnlqy, 46 In 182'.), Dr. Morion illustrated a soctloii of CrotJiceoiis rocks, 27 8-12 feet ill liei<3;lit, found in ji blulf, on the niarjfin of Crosswiclc's (hoek, New- Jersey, and separated the Cretaceous of New Jersey and Delaware in- to the lignite strata and the marl. He relied, in determining the Cretaceous age of the rocks, upon the genera Terehratula, Oryphwn, Exogyrd, Ammonites^ lincnlites and Beleinnifes. He described,* from an excavation for the Delaware and Chesapeake canal, Ostreafalcatu, and from other places, Terehratula harlani, T. frayilis^ T. sayi^ Gryphcea miifdhilis and G. vomer. In 1830,f he published his Synopsis of the Organic Remains of the Feiruginous Sand Formation of the United States, with geological re- marks. He treated of the distribution of the strata, and mentioned many localities in the eastern and southern States where they are ex- posed, and also discussed the mineralogical characters of the marls. He described Belemtiites americanun, B. ambiyuus, CucullcBa vulgaris, now Tdonearca vulgaris, Ammonites delawarensis, A. vanuxenii, Spatan- gus Stella, Ananchytes crucifenis, A. cinctns, A. Jimbriatus and An- thophyllum atlanticiim, now Monfivaltia atlantica. He also deter- uiinedthat two species, figured in Sowerby's Mineral Couchology, under the names of Chama heliotoidea and (J. eonica, belong to Say's genus hlxogyra. Sowerby soon after adopted his determination, which was the first instance in which the genus of an American author was adopted in Europe, where it required the separation of the species which had been referred to an older genus. In 1833,J he published a Supplement to his Synopsis, in which he il- lustrated and described Bostellaria arenaria, now Anchura arenaria, TorniteUa hullata. Conns gyratiis, Cytherea excavata, now Cyprimeria excavata, Cardita decisa, Clavagella armata, Plagiostoma gregale, now Spondylus gregalis, P. pelagicnm, now Lima pelagica, Pecten perplanus, P. venastas, Anomia argentaria, Gryphoia plicatella, Os- trea falcata, var. nasuta, 0. mesenterica, 0. tortuosa, 0. iirticosa, * Jour. Acad. Nat. Sci., vol. 6, part 1. t Am. Jour. Sci. &. Arts., vols. 17 & 18. I Am Jour. Sci. & Arts., vols. 23 & 24, ; > 46 C'retaccoui*. Teredo tihialis, now PolfirfJirim fifn'rilfs, Terchrahiln /iftrlani, var. dt's- coit/ca, T. hfirln(((tiffns iin(jii/d. Some of the species whioli ho (lesei'ibed iijt this time, iiiul rofenod to tlieCretiieoous, iire now rcpirded ns of Eocene njj^o. Anion^' those we may mention, Nvmmiilif.es mnntelh\ \y\\\v\\ litis been the sul)joct of much discussion, and is now referred to D'Orbigny's jjjonus OrhifoideH, and classed with the Pro- tista, In 18;I4, his Synopsis appeared, illustrated with nineteen plates, and havintr an appendix, containlne, which has been heaped up by the genius and industry of the naturalists of l)oth hemispheres." lint the carefulness with which the work was prepared, and the sound discrimination and learning displayed upon every page, arc so obvious that one is struck witii astonishment, in comparing it with the peurile and liy|)othetical essays which emanated, at that time, from the colleges and professed teachers of geology. It was not only a valuable contribution to knowledge, prepared by -^ physician, during the constant interruptions of a professional life, it was the best work which had appeared, at that time, upon An. ...an Geology, and one that will continue to be a standard of science for many decades to com''. He separated the Cretaceous into two parts, the lower. Ferruginous Sand, and the upper, Calcareous Strata. The mineralogieal characters of the Ferruginous Sand are extremely variable, consisting, for the most part, however, of minute grains, collected into friable masses of a bluish or greenish or grayish color, the predominant constituents of which are silex and iron. Iron pyrites is found in profusion; succinite, lignite and spheroidal masses, of a dark green color, and compact, sandj' structure are not uncommon. The calcareous strata consist of several varieties of carbonate of lime, the principal of which are as follows: an extremely friable mass, containing silex and iron, and about 37 per cent, of lime, composed almost entirely of disintegrated zoophytes ; a yellowish or straw colored limestone, full of organic remains ; a granular or subcrystalline limestone, intermediate in structure between the former two; and a white, soft limestone, not harder than some coarse chalks and replete with fossils. All these va- rieties are occasionall}' infiltrated by silicious matter, and contain Menozolc finil Ca'nozon; Otohnjij oiitl Piilwoiifuloi/;/, r musses of elicil, iiiul als(» |)ri!ScMit some iiiipciiniiu'i'S of tlu' ^^ri'cii ;^riiiiis HO fluinicteristic of tlio ;nljiuL'Ul marls. The ('rotiiecous formation is unofiiiivooally rcroj^iiizcMl iu New Jersey, from whence It r.my be loeally traced Lhroiieen fonnd in the latter State that have not been noticed in the former, and vice versa.'^ The calcareous strata appear to be much less extensively distribut- ed than the friable n arls, and present considerable dilference in their organic characters, and always when observed form the overlying beds of this formation. Two sections of the strata, as observed in Delaware, are furnished. Localities of exposure are mentioned in Maryland, Virginia, North and South Carolina, Georgia, Alabama, Mississippi, Tennessee, Louisiana, Arkansas, Missouri, and in the level country between the Missouri river and the Rocky Mountains. Ho described: NaiitUus dekayi, Ammonites navicularis, A. pet- echialis, A. telifer, A. conrndi, now Scaphites conradi, A. conradi, var. yulosus, now Scaphites conradi, var. yulosus, Scaphites reniformis. A, vespertinus^ now Jlortoniceras vespertinum, A. syrtalis, now Placenti- ceras syr talis, Bacalites asper, B. carinatus, B, colunma, B. labyrin- thicus, Hamiles arciilus, H. torquatus, II. traheatus, Trochus leprosas, noAV Phorus leprosus, Deiphinnla lapidosa, now Angaria lapidosa. Turritellaencrinoides, T. vertebroides, Scalaria sillimani, S. annalata, Rostellaria pennata, JSlatica ahyssina, now Gyrodes abyssina, JY. petrosa, now G. petrosus. Cirrus o'otaloides. Patella tentorium, Ostrea cretace'a, 0. plumosa, Pecten craticula, Plaouna scabra^ Inoceramus barabini, I. alveatus, Avicula lariiies, Pectunculus australis, now Axinoia australis, P. hamula, now A. hamula, Area rostellata, now C'ibota rostellata, Cucullcea antrosa^ now Idonearca antrosa, V. vul- m 'I'M I I ! iM :i-i! •I ^i! 48 Cretaceous. M W \t l» !'■''' yarfs, notv /. vulgaris, Crassatella vadosu, Pholadomya occidentalism Trigonia thoracica, Venilia conradi, uovv Veniella conradi, Tercbratula floridana, Serpula barbaia, Hamulus onyx, C'assidulus wquoreus, Clypeaster geometricus, Flustra sagena, now IHiophloia sageiia, Eschara digitata, Alveolites capularis. Turbinolia inauris and Gryphoia pitcheri. The latter species was collected by Dr. Z. Pitcher, on the Kiamechia, a stream v.hich empties into the Red river, a few miles above Fort Towson, when on a tour with a small military force, marking out a road from Fort Smith to Fort Towson. Dr. Pitcher and M.Jules Marcou referred the rocks to the Jurassic, and JNIarcou claims that the species is distinct from that which abounds in the Cretaceous of Texas, and farther west which is now so universally referred to this species. The weight of authority, howev'er, is in favor of the identity of the fossils, and the Cretaceous age of the specimens described by Dr. Morton. lu 1835, in an appendix to his Synopsis of Organic Remains, he separated the Cretaceous into upper, middle and lower divisions. In the upper division he placod the Cretaceous of South Carolina, and the Nummulite, o»' Orbitoides limestone of Alabama, which has since been regarded as of Eocene age. The middle division is partially seen at Wilmingtoii, North Carolina, and to a considerable extent in New Jersey. The lower division embraces the vast Ferruginous strata of the Atlantic and Southern States. He enumerated the fossil species which he regarded as most characteristic of these divisions, and de- scribed Plogiostoma echinatum, now Spondylns echinatus. In 183l, when Meek and Hayden, in accordance with the laws of nomenclature, gave them the following geographical names: No. 1, Dakota Group; No. 2, Fort Benton Group; No. 3, Niobrara Group; No. 4, Fort Pierre Group; and No. 5, Fox Hills Group. They described from No. 5, at Fox Hills, Pecten rigida, now Syn- cyclonema rigidum, from the Bad Lands of Dakota, BacuUtes grandfs; from No. 4, at the Great Bend of the. Missouri, below Fort Pierre, Avicula haydeni, Tnoceranuis convexits, I. tc 'j'Uneatus, T. subloivls^ Nucula subnasiUa, now Nnculana ifuhna'ni.u, Buccinum vinculum, now Truchytriton vinculum, Ammonites complexus, Turrilites cochleaius, now Ileteroceras cochleatum: from Sage creek, Nucula ventricosa, now Yoldia venfricosa, Crassatella evansi, Lucina subun- data, Dentalium gracile, Actoion concinnus, now Cinulia concinna, Fusus tenuilineatus, now Closteriscus tenuiUneotus, Katica concinna, now Lunatia concinna, JSFatica paladiniformis, now Amauropsis, paludiniformis, Funu.s con.strictus, now Odontobasis conslricta; from No. 2, near tlie mouth of Vermilion river, Tnocernmus frag His \h'on\ below the mouth of James river, Cytherea orbiculata, now Callista orbiculata and C tenuis; from No. 1, at the mouth of Big Sioux river, on the Missouri, Pectunculus siouxensis, now Trigonarca sioiixensis. Dr. Geo. G. Shumardf found the Cretaceous rocks at Fort Washita, and extending from there uninterruptedly to the southwestern boun- dary of the Cro 5« Timbers, in Texas. It usually consists of grayish yellow sandstone, with intercalations of blue, yellow and ash colored clays, and beds of white and bluish white limestone. The limestone reposes on the clays and sandstones, and in some places attains a AW 1J = V '■' Mem. Ain. Acad. Arts '^:as into Mexico, near the Mexican =;ettlemcnt of San Cuvlooi. The voek exposure exhibits a ^ ory variable dip, i.ostly inclined toward the west, occasionally at a very sharp angle. I*; rises nt various points in the adjoining table- land, forming ochreuus coloiiid rocky bluffs, where at several points the gravelly table-land is seen to rest unconformabl}' on the sharply- tilted strata. Further down the river, in an eastern direction, the Cretaceous assumes a nearly horizontal position, and a closer texture. It is here seen overlaid by a variable sheet of dark-colored lava rock. This sheet of igneous rock conforms closely to all the inequalities of the underlying limestone, exhibiting, in tbo walls of the Canon below, a distinct line of separation traceable for a longdistance. The wester- ly dip of the Cretaceoi's underneath grad;'.'illy tliii.s out this upper igneous capping, which finally disappears, and solid limestone walls continue along the lino of the river. At one point on the line of the trail loading round the broken ranges of the mountain ledges, directly bordering the river, to reach its bed ^;iiii:";!!' Mixozoic. and Civtnizuic (icolnifi/ and Ptthvontoloyy. (11 some ('i|;ht iniUn holow tlio C/oiuuiulic Konl, tlio sides of a th't'p washed ravine bring to view tlie wuceesslve and relative tliieUnessoCtlie rocks. We here SCO the upper iiienihers of the ('retaeeons roiks r<»rinin,t? tlio tabled siininiits oC the adJoiniii5 < pa s « H (i< O >0 S? «^ m O J?; o H H (?: • M D w Eagle Pass is an open country, occupied by low swells of Cretaceous limestone, thus merging into that character of country pertaining to the region of central Texas. Prof. James Hall, to whom the minerals and fossils collected by the ^ tundary Commission were referred for geological examination, com- pared the Cretaceous of Texas and New Mexico with that of Nebraska anc( the eastern states. He furnished the followin.y section of the successive beds comprising the Cretaceous formation of New Jersey, which had been communicated to him b^ Prof. Geo. H. Cook for comparison, to wit: 8, Greensand, Thiiid ou Uppeu Bed. [Probably of Eocene Age.] This bed admits of a triple divi 'ion, the central portion is nearly destitute of fossils, while those of the upper and lower divisions are mostly dissimilar. 7. Quautzose Sand, resembling Beach Sand. This bed is (so far as known), quite destitute of fossils. f G. Greensand, Second Bed. 1 {a) Yellow limestone of Timber Creek. Characterized by Eschara digitcita, Montivaltia atlantica^ Nucleolltes crucifer, Ananchyies ductus, A. fimbria t as, Morton. (6) A bed of nearly unchanged shells. Among the character- istic fossils of this bed are Gt'i/phcea vomer, O. convexa, and Tere- hratula harlani. (c) Greensand, etc. CucuLloia vulgaris is the most characteristic fossil of the lower division. 5. QuARTzosE Sand highly Ferruginous throughout, and Argillaceous in its upper parts. This rock is sometimes indurated or cemented by oxyd of iron. Exogyra costata, Ostrea larva, Belen^^-'^'tella mucronata, Pecten [Neithea) quinqu'ecostfUus ; and m.' ny other fossils mostly in the condition of cas :s of the interior, or impressions of the exte- rior. 4. Greensand, First or Lower Bed. Several subdivisions may be recognized depending on the char- acter of the marl, etc. Exogyra coi'tata, Ostrea larvc, Belemni- tella mucronata, T'erehratuln sayi, (Gryphoia cnnve^a and G. mutabilis), Ostrea vesicular is. 3. Dark Colored Clay, containing Greensand in Irregular Stripes and Spots. Ammonites delawarensis, A. placenta, A. conradi, Baculites ovatus, casts of Cardium. Masozoic and Cwnozoic Geology and Palmontology. 63 2. Dark Colored Clay. [Position of beds Nos. 2 and 3 of the Ne- braska section.] At the present time the evidence tends to show that No. 1 of the Nebraska section is represented b}' Nos. 1 and 2, and that Nos. 2 and 3 of the Nebraska section are wanting-, and would find a place between Nos. 2 and 3 of this section if existing. This bed contains large quantities of fossil wood (no animal remains are known to occur in it). 1. Fire Clay and Potter's Clay. This bed contains fossil wood, and numerous impressions of leaves; but no animal remains. In making the comparison of the strata he placed a large part of the Cretaceous fossils of tlie boundary survey in the same parallel with beds Nos. 2 and 3 of the Nebraska section, and below those bods in New Jersey and Alabama, which contain Baculites ovatus, Kautilus dekayi and Ammonites placenta. He described from Leon Springr., Pyrina parry I. Prof. T. A. Conrad described, from between El Piiso and Fron- tera, Turhinolia texana, Cuculla'a terniiualfs, Area siihelonyata, Car- dluni mediale, Gytherea texana, Ostrea vellicata, JSfodosaria texana; from Leion Springs, Trigonia texana, Protocardla Jilosa, Cardita em- inula, Lima leonensis, Cytherea leonensis. Ammonites geniculatus, A. leonensis, Gapsa texana, Terebratala leonensis, Turritella leonensis; from Rio San Pedro, Cardiam congcstam, Natica collina, iV. texana, Rostellaria collina, Buccinopsis parry i; U'dvaDvy creek, Mexico, Os- trea cortex^ O. multilirata; from Turke\' creek, Leon and Eagle Pass roads, Pholadomya texana; from Jacun, three miles below Laredo, Ostrea robusta, Ammonites pleurisepta; from other places, Gorhida occidentalism Inoceramus texanns, Astarte texana, Plicatiila incongrua, Ostrea bella, 0. lugubris, Tarritellp, plan Hater is, Kerinea schotti, and Gardita subtetrica. Evans and Shumard* describee^' from Nebraska, Avicula nebras- cana, Limopsis striato-punctata, Cardittm subquadratum, and G. ra- rum, now Protocardia siibquadrata^ and P. rara, Area sulcatina, now Nemodon sulcatinus, Leda fibrosa, now Ifeoira fibrosa, Mytilus meeki, now Volsella meeki, Ostrea sublrigonalis^ Pleurotoma minor, Fusiis nebrascensis, Turritella multilineata, Eostellaria americana, now An- chura americana, and Ammonites galpini. Meek and Haydenf described, from the Great Bend of the Missouri, 'W\ '•'' Trans. St, Louis Acad. Sci., vol. 1. t Proo. Acad. Nat. Sci., vol. 9. 64 Cretaceous. and other places in Nebraska (Fort Pierre Group), Ptychoceras mor- toni^ Fusus subtiirrltas, now Pyrifams subturritas, t\ interfrxtus, now P. intcrtextus, Xylophar/a eleyantula, now Turnus eleffctntulus, X. stunpsont, now T. stimpsorii; from (Fox Hills Group), near the mouth of Heart river, Fusus vau(jhni\ and from other parts of Nebraska, Fusus (?) sca)'bo>'ou(/Jil, now Fdsciolaria scarborouyhl, Pholadomya subuentricosa, Cyprina cordatn, now Sjjhcerlola (?) cordaUt, C. com- pressa, C. siiotumkla, C. ooata, Pect.inculus subimbricatus, now Axinma subi'mbricatu, Ostrea iranslucida, Ilemiaster huntphreysanus\ from the month of Judith river, T'itHna obliqua, Pianorbis amplexus. Helix occidentah's, now Hyalina occidentalism II. vitrinoides, now H. vetusta, .Melania omitta, now Goniobasis omitta, 31. subtortu- osa, now G. subtortuosa, 31. subkevis, now G. siibla;vis, 31. invenusta, now G. invenusta, Unio danai, IT. deivei/aiuis, IT. subspatulatus^ Ostroia glabra; from the Fort Union Group, Lignite beds at Fort Berthold on the Missouri river, Pianorbis frar/ilis, now P. j^lanocoii- vexus, 3Ielania tenuicarinata, now Goniobasis tenuicarinata, 31. warrenana, now Ilydrobia tvurrenana; from the Fort Benton Group, at the mouth of Vermilion river, Serpula tenuicincta; from the Da- kota Group, near the mouth of Vermilion river, Solen dakotensis, now PhoreUa dakotensis, and Cyprina arenaria, now Cyrena arenaria. The roeks* of the Lower Cretaceous, in Mississippi, consist princi- pally of stratified sand, mixed with a large proportion of silicate of iron or glauconite, which imparts to it a greenish color of different hues, and has given origin to the very appropriate name of greensand. The indurated greensand is generally full of fossils. It is exposed in the western part of Tishamingo, eastern part of Tippah, northwestern part of Itawamba, northeastern part of Pontotoc, and northeastern part of Lowndes county. The Upper Cretaceous has sometimes been called the rotten lime- stone, and occupies a larger area than the lower division. It occupies part of Kemper, Noxubee, Lowndes, Ocktibbeha, Chickasaw, Monroe, Pontotoc and Itawamba counties. This division is also highly fossil- iferous where well exposed. The estimated thickness of the whole is placed at from 1,200 to 1,500 feet. DrLeidyf described, from Columbus, Miss., TIadrodus priscus; from Nebraska, Phasganodus dims, and from the greensand of New Jersey, Pycnodus robustus. *' Geo. of Miss. t Proc. Acad. Nat. Sci., vol. 9. Mesozoic and Ccenozoic Geology and Palasontoloffi/. 65 In 1858, Dr. Geo. G. Shurnnrd* described the Cretaceous rocks near the mouth of Delaware Crock, ou the Rio Pecos, in New Mexico, where he found a tiiickness of 9G0 feet. Tlie first IOC foet consists usually of a hard limestone, of a light cream coIcm* and ' arth}' texture, and con- tains numerous spheroidal cavities, froni a fo irth to a half an inch iu diametei', which are sometimes partiall3' (ilhd with loose, ferrui^inous earth. In other places it is softer and lighter colored, resembling im- pure chalk. Beneath this limestone, deposits of gypsum, clay and sandstone o(;cur. In some places the strata are much disturbed, and are found dipping in opi)Osite directions, at angles of 40° or 50°. He also referred to the Cretaceousf certain stiata in the bluffs of the ^liss- issii)pi, above Commerce, Missouri, having a thickness of 158 feet, but no fossils were obtained. The Cretaceous rocks;]; occupy a belt across the State of Alabama, from 50 to 100 miles in width. The counties, either in whole or in l)art, exposing these rocks on the surface, aie Barbour, Russell, Pike, Macon, Montgomery, Butler, Lowndes, Autauga, Wilcox, Dallas, Perry, 3Iarengo, Greene, Choctaw, Sumpter a:ul Pickens. T. A. Coiirad§ described, from Tippah county, Mississippi, Fhola- domya tippana, Periploma appUcata, SiUqiiaria biplicata, now Lep- tosolen hiplicatus, Leyinnen elltpticus, L. appressus, Dosuita densaia, Mereti'ix tippana, now Aphrodina tippana, Papyridca beUa, Car- dlum ripleijen.se, C. spilliaani, C. tippaaum, Opis bella, 0. hicarinaia, Tellhia riplei/ana, JS^uctda percrasna, Cibota liniea, CucuUoia capax, C. tippana^ now Idonearca tippana, Dreissena tippana, Pinna laq- uata, Gervlllia ensiformis, Lima acutilineata, Inoccraniiis argeu- teus, T. costellatus, Ostrca confragosa, O. peculiaris^ O. denticnlifera, Exogyra interrupta^ Pidviniies argentoa, Anomia sellmformis, Strom- bus densatus, now Pugncllus densatus, Aporrhais decemlirata, now An- chura decemlirata, Ilarpago tippanus, now Pterocerella tippana, Bimella < rvilirata, Conus canalis, Drillia tippana, D. nocemcostata, Turris ripleijana, Fusus novemliratus, F. bellaliratus; Pyrifusus sub- densatiis, Ficus octoliratus, Rapa siipraplicata, Volutilithes cretacea, now Volatomorpha cretacea, Chemnitzia distans^ C. interrupta, Tri- chotropis cancellaria^ Turritella altilis, T. tippana, Lunatia rcctila- brnm, Solididus linteus, Bidliopsis cretacea, BacuUtes spillniani, B. tippaensis, Scajihites iris, and Cytherina tippana. Meek and Hay den || described, from (now the Fox Hills Group) Long '■' Trans. St. Louis Acad. Soi. vol. 1. t Proc. Am. Ass. Ad. •''ci, (J Jour, Acad. Nat. Sci., 2d ser. vol. 3. t Goo. of Ala., 1858. II Proc. Acad. Nat. Sci. i 66 Cretaceous. Lake, Ncbi'aska, Corbuht inornata, Pholcis cuneata, now 3Iartisia cu- neata and Actwon altcnuata. From (now the Fort Pierre Group) near Fort Clark, Teredo (jlohosa, Jlelicnceras forf.um, now Ilebcrocerds torf,um, TiirrilUes cochleaftts, now Ileteroceras cocldeatnvi^ 11, tcnvicostatum, Tarrilites ximbllicalus, now U. xnnbilicatam, and Aiicijloceras uncnm. From (now the Fort Benton Group) Fort Benton, on the Upper Mis- souri, Iitoceramus icmboiinfns now Voloiceramns umbonalas, and from th(! Black Hills, Scophites larvcvformis. * Dr. Leidy described, from the marl of Haddonfield, Camden county, Ncvv Jorse}', Jladrosavrus fovUci. V. B. Meek* described, from Vancouver's Island, Kucula traskana, Area a-qnila feral is, A. vancouvertnsis, CariUam scitulum, Phola- domya borealis, P. subelonr/ata, Trir/onin evansana, lliracia occiden- talis, T. siibtruncata, Dentalium nanaimoense, and Ammonites ramosus. Dr. B. F, Shuinardf described, from the same island, Inoceramus vancfHiverensis, Pinna calamitoides, and Pijrula (jlabra. Prof. E. Emmons]; described, from the Greensand of North Carolina, Sphcnodus rectidens, and Bclemnitella compressa. Prof. Oswald Heer,§ of Zuiich, Switzerland, described, from Ne- braska, Liriodendi on meeici, Sapotacitcs haydeni, Le[/uminosites mar- conanits, i?ow Biimelia marcouana, Popnlus cyclophylla, now Cissites ci/clopfiyUa, Phyllites obcordatiis, and P. obfusilobatus. In 18r)9, Prof. Henry Y. IIind| found the Cretaceous rocks in posi- tion on the Little Souiis River, in longitude 100° 30' W., and on the South Branch of the Saskatchewan, in longitude 106° 35' W., and be- tween these widel}' separated points in many places on the Assinibolne, the Qu'Appelle, and their afthients. Fifteen miles from the mouth of the Little Souris, the rocks consist of a very fissile, dark blue argilla- ceous shale, holding numerous concretions, containing a large per cent, age of iron. This exposure is 70 feet thick, and the layers are per- fectly horizontal. The whole is supposed to be of the age.of the Fort Pierre Group. The Cretaceous of this latitude appears to repose directl}' n[)on the Devonian, as the former is found undisturbed and nearly horizontal at altitudes from 400 to 600 feet above exposures of Devonian age, recognized in situ 30 miles to the east. Prof F. B. Mcek^ described, from the Little Souris River, Anomia flemingi, Inocercunits canadensis, Leda hindi, now Nucalana hindi, and '■' Trnrs. Alb. Inst., vol. 4. t Trans. 8t Louis Aoad Sci., vol. 1. X Geo. Sur. N. Carolina. I Proc. Acad. Nat. Sci. II Assiniboine and vSuskatchcwnn E.xpl. Expcd. H Rep. on Assiniboine and Sasliatehewan E.\pl. Expcd. Mesozolc and Camozolc Geology and Palaeontology. 67 from the valley of Mackenzie's li\\{i\\ Ammonites, barnstoni; and A, hillings i. Prof. Leo. Lesquereux* described, from Vancouver's Island, and Bell- Ingham Bay, Populus rhomhoidea, Salix islnndicus. Quercus benzoin, Q. multinervis, Q. evansi, Q. gandini, Q. ptatinervis, Planera diibiai Oinnamomum heo'i, now Daphnogene heeri, Persoonia oviformis, and Diospyros lancifolia. In I860, Dr. B. F. Sluimardt subdivided the Cretaceous strata of Texas in descending order, as follows: 1. Caprina limestone, having a thickness of GO feet, and consisting of a yellowish white limes'one, usually massive, sometimes of a finely granular structure, and some- times made up of rather coarse, subcrystalline grains, cemented with a chalky paste. It has an extended geographical range. 2d. The Co- manche Peak Group, having a thickness of 300 to 400 feet, and made up of soft, yellowish and whitish chalk}- limestone, and buff and cream- colored limestones of greater or less compactness, being highly fossilif- erous, and having a great geographical extension. 3. The Austin limestone and fish bed, having a thickness fiom 100 to 120 feet. The Austin limestone consists of cream-colored and bluish earthy limestones, and the fish beds of shaly layers of dark-blulsh-gray calcareous sand stone. This is supposed to represent Nos. 4 and 5 of the Nebraska section, by Meek & Haydcn. 4. Exogyra arietina marl, having a thick- ness of 60 feet, and consisting of an indurated blue and yellow marl with occasional bands of gray limestone, and thin stams of selenite in- terstratified. 5. Washita limestone, having a thickness from 100 to 120 (eet, a wide geographical range, and consisting of white, yellow, gray and blue limestones, some of which are moderately hard, and others disintegrate rapidly. This is supposed to be parallel with the lower part of No. 3 of the Nebraska section, by Meek and Hay den. 6. Blue marl, having a thickness of 50 feet, and consisting of an in- durated arenaceous marl, of a schistose structure, with small nodules of iron pyrites and irregular masses of lignite disseminated through it. It is not observed south of Gra3'son county, and is supposed to correspond with No 2 of the Nebraska section. 7. Caprotina lime- stone, having a thickness of 55 feet, and forming the basis of what is called the Upper Cretaceous Group. It is composed of light gray and yellowish gray earthy limestone, with intercalated bands of yellow marl and sometimes flint, and is exposed at the base of the hills near Comanche Peak, and underlying the Washita limestone near the Colo- * Amor. Jour. Sci. and Arts, 2d Scries, vol 27. t Trans. St. Louis Acad. Sci., vol. 1. es CretaceouN, I ' i rado, Tit the foot of Mt. Bonnell. 8. The Arenaceous Group and fish bed, having a thickness of 80 feet, and consisting of light yellow and blue sandstone, and beds of sandy cla}', with crystals of selenite and some lignite. This is supposed to be the same as B, C and D of the Pjramid Mount Section of Prof. Marcou, and by him referred to the Jurassic period, and to be equivalent to No. 1 of the Nebraska Sec- tion, y. Marly Clay or Red River Group, having a thickness of 160 feet, and supposed to represent the lower part of the Pyramid Mt. Sec- tion, which Prof. Marcou referred to the Trias. He described Nautilus texanus, Ammonites inaiquiplicatus, A. swallovi, A. meekanus. A. graysonensis, A. brazoensis, Scaphites ver- miculus, Ancyloceras amiulatiim^ Baculites gracilis, Cerithium bos- quense, Phasianella perovata. Avellana texana, Natica acutispira, Neritopsis biangulatus, Venus sublamellosus, Cardium choctawense, now Protocardia choctaivensis, C coloradoense, C. brazoense, now Protocardia brazoensis, Cytherea lamarensis, now Dione lamarensis, Tapes hilgardi, Area proutana^ Liicina sublenticular is, Nucula hay- deni, I^. serrata, Corbula graysonensis, C. tuomeyi, Pachymya austin- ensis, Panopoea neivberryi^ P. subparallela, Jnoceramus capulus, Ger- villia gregaria^ Janira lorighti, Ostrea belliplicata, O. quadriplicata, Cidaris hemigranosus. Wm. M. Gabb* described, from Prairie Bluff, Alabama, Chemnit- zia meekana, Straparollus subplanus, Sconsia alabamensis, Cancellaria alabam.ensis, now Turbinopsis alabamensis, and Bulla macrostoma; from the marl of New Jersey, Actmonia naticoides, now CinuUa nati- coides, Phasianella punctata, Volutilithes biplicata, now Bostellites biplicatus, V. bella, noiv P. bellus, V. nasiita, now P. nasutus, V. con- radi, now B. conradi, Fusus retifer. Papa elevata, Morea naticella, Bulla recta, Mysia gibbosa, Dione delawarensis, Crassatella delawar- ensis, V. monmouthensis, Cardita subquadrata, Leda pinniformis^ now Nucidana pinnijormis, L. protexta, now N. protexta, Cultellus cretaceuSj Pecten burlingtonensis ; wfrom Tennessee, Volutilithes saffordi, and Cardium abruptum; from New Jersey, Actceonina bipli- cata, now Solidula biplicata, Solarium nbyssinus^ now Margaritella, abyssinus, Volutilithzs abbotti, Turbinella subconica, T. parva, Can- cellaria septemlirata, Purpuroidea dubia, Fusus trivolvis, Papa pyruloidea^ Pleurotoma mullicaersis, Area quindecemradiata, Cibota multiradiata, and Leda angulata, now Nucularia angulata, Desma- tocium trilobatum, and from Eufala, Alabama, Cassidulus micro- coccus. '■•' Jour. Acad. Nat. Sci. 2d. Ser., vol. 4. Mesozoic and Cmnozoic Geology and Pahnontoloyy. by Wm. M. Gabb* des(M'ibetl, from Eufaulti, Alabama, Fasus holmesnn- us, C'ancelldi'ia euj'aulensis, Dentalium ripleyanum, Venus meekana Astarte octolirata, Triyonia eujaul'^nsis, Axincen rotundnta, Nucula distortft, iV". etffaulens/s, Area enfanlensi's, now ISfemodon cufaulensis, Hamidns major; from Ilurdoinan count}', Tennessee, Neptnnea im- pressa, Fasclolaria soffordl, Turritella hardemanensis, T. pumila, T. sajfordi, T. tennesseensis, Venus ripleyana, Corbula subconipressa, C. crassipUcata, Modiola sajfordi, now Volsella saJford>\ Area saffordf, Ostrea erenuUmar(jinata; from New Jersey, Rostellaria rostrnta, now Anchiira rostrata, Cypro'.a niortoni, Lunatia ludlL Pholas cretacea, now Martesia cretacea^ Teredo irregularis, now Polarlhrus irreyu- laris^ Gastrochania umerieana, now Polarlhrus americanus, Isooardia conradi, now Opis conradi, 3Iodiola ovata, now Volsella ovata^ Leda slackiana, now N^icidana slackana, Serpida habroyramma, Denfalina ptdchra, now Phonemus pulcher; from the Indian Territor}', near the Choctaw Mission, Chemnitzia occidentalis; and from Oregon, Discoidea oceidenlalis; Gabb and Horn described, from Hardeman county, Ten- nessee, Platytroehus speciosus; from Prairie Bhitf, Alabama, Flabellum striatum; from New Jersey, Trochosmilia conoidea, Acerviclausa ver- micularis, Heterocrisina abbotti, now Bicrlsina abbottl. Hippothoa irreyxdaris,\ Ccllepora carinata, now Iteptoporina carinata, C. typica, now Escharifora typica, Reticulipora sayena, and 3Iulticrescis par- vicella. T. A. ConradJ described, from Barbour county, Alabama, and Tip- pah county, Mississippi, Pholadomya anteradiata, P. papyria, P. postsulcata, Sanguinolaria cretacensis, Tellina eufaidensis, T. lim- atula, T. eborea, Dosina depressa^ now Cyprimeria depressa, D. ob- liquata, 3Iysia pur His, now Tenea par His, Cardium linteum, now Cymbophora lintea^ Crassatella lititea, C. pteropsis. Linear ia met- astriata, KeVia cretacea, Sphcerella concentrica, Crenella sericea, Cuculhea maco.iensis, now Triyonarca maconensis, Nucula cunei- '■' Jour. Aciid. Nat. Sci., 2d ser. vol. 4 t Proc. Acad. Nat. Sei. t Jour. Acad. Nat. Sci., 2d ser. vol. 4. '*;- I, It 70 Cretaceous. : J ' frons, ^. percBquali. Leda lonyffroDs, now Kuculana loiujifrons, Venilln trapezoidea, now Veniella trnpezoideci, Cardiinn eiifanlense, Dione eufaulensifi, Astarte crenalirata, Corhula eufaulensis, Plica- tula saffordi, P. tetrica, Pecten argiUenttLs, P. inis.sissipjiiensis, P. simplicius, now Syncyclonema s.'mplidum, Ihirrilites sjiiniferus. An- chura abrupta, TurriteUa trillra. Daphnella eufaulensis, T), liniea, D. suhftlosa, Dn'llia dfntans, Fusus tippanus, Strepsidura ripleyana, Volutilithes eufaulensis, Actaion modicellus, Chemnitzia corona, C. me lanopsis, C. spillmani, C. laqueata, C. triyemmata, Pyrojisis perlata, yeritella densata, Gyrodes alveatus, G. crenatus, Turhinopsis hilyardi. Tuba bella, now Spironema bellum, Morea cancellaria, Thylacus ere- taceus, Placunanomia saffordi, Cassldulus abruptus^ and C. subquad- ratus. Prof. E. W. Hilganl* subdivided the Cret.iceous rocks of Mississippi into four groups as follows : 1. The lowest, the Eutaw Group, as char- acterized by Tuomey, near Eutaw, Alabama. 2. Tombigbee Sand Group. 3. Rotten Limestone Group. 4. Ripley Group of Conrad. The Eutaw Group consists of bluish black, or reddish, laminated clays, often lignitic, alternating with, and usually overlaid bj-^ non-effer. vescent sands, mostly poor in mica, and of a gray or yellow tint. It contains beds of lignite, and rarely other fossils. It is displayed at a few places in Tishamingo, Itawamba, Monroe, and Lowndes counties. The Tombigbee Group is usually a fine-grained micaceous sand more or less calcareous, usually of a greenish tint, but not unfrequently gray, bluish, black, yellowish and sometimes even orange red. The greenish tint is imparted to these sands not by greensaud grains, as is the case in the marls of the Riple}'- Group, but is caused by a greenish incrustation, covering thinly a portion of the quartz grains, but the presence of glauconite in the incrustation has not been detected. Cla3's and non-calcareous sands are subordinate to the greenish sand. This Group forms a narrow belt on the western exposure of the Eutaw Group, and extending from Lowndes county through Monroe, Itawamba and Tishamingo, to the southern border of Tennessee. The Rotten Limestone Group possesses the same characteristics as- cribed to it by Tuomey in Alabama, and appears as a soft, chalky rock, of a white or pale bluish tint, with very little sand ; consisting of vari- able proportions of fat, tenacious cla^-, and white carbonate of lime in crystals extremely minute, and with some shells of infusoria. It is * Geo. of Miss. Jfesozoic (tnd Cwnozoic Geology and Pnlaionf.olof/y. 71 I \4 generally highly fossUiferous, and irregular, roiuulecl nodules of iron pyrites of a radiated structure called "sulphur balls" are common. It is of great thickness on its southwestern border in Chickasaw^ Octibbeha, Noxubee and Kemper counties, where borings have been made in it from 700 to 1000 feet, but there is a gradual thinning out northward, througii Pontotoc, Itawamba, Tii)pah and Tishamingo counties to the line of Tennessee. Tiie surface area of this sub- division in Mississippi is greater than that of the other three com- bined. The Ripley Group forms the border of the western exposure of the Cretaceous, from a point in Chickasaw through the central part of Pontotoc, the eastern part of Tippah and western part of Tishamingo to the south line of Tennessee. It consists of hard crystalline lime- stone, more or less sandy and glauconitic, vvhicii forms the highest strata; and bluish micaceous marls, more or less sandy, and often in- terstratified with subordinate ledges of sandy limestone, which latter become less and less frequent as we descend in the series toward the strata forming a transition into the Rotten limestone. Meek and Haydeu* described, from (Fort Benton Group) the mouth of Vermilion river. Ammonites oermilionensis, now Jfortoniceras ver- milionense ; from near the Black Hills, Scaphites warreni ; from Little Blue river, Inocernmus aviculoides, now I. problematicns, var. avica- lokles ; from (Fox Hills Group), Moreau river, PhyUoteiithis suhovn- tus, DentaUitm pauperculum^ now Entalis paupercula, and Cylichna soitula ; from 20 miles below the mouth of Cannon Ball river, Tellina formosa^ now Linear la fo>'mosa ; from the north branch of Cheyenne river, Cyprina humilis, now Veniella humills ; and from Long Lake^ Avicula subgibbosa, now A. Unguiformis, var. subgibbosa ; from the mouth of Judith river (Judith river Group), Helix evansi, now Hyidina evansi; from the mouth of Grand river, Sphan'iiim planum, S. recticardinale, Cyrena cytheriformis, now Corbicula cytheriformis^ and Inoceramus subcompressus, now /. cripsi., var, subcompressus ; from (Fort Pierre Group) the head of the south branch of Cheyenne River, Helicoceras angulatum, now Heteroceras angulatum, Ammon ites placenta, xav.intercalaris; now Placenticer as placenta^ var. inter- calaris, from the Yellow Stone river, Scaphites nodosns^ var. plenus, Aporrhais parva, now Anchura parva, A. siiblaevis, and 3Iactra gracilis; from Fort Clark, Teredo sell if or mis ; from White river, Inoceramus vamixemi, I. balchi; from Bijou Hill, Anoniia sublvigon- '^■i ■ '■ Proe Acad. Nat. Sci- I. 79 Cretaceous, i Hi alis, nntl from tho i^ront bond of tlio ^Missouri river bolow Fort Pierre, Osfrea inorrmfa. From (Niobr.'irn Group) noiir the mouth of tlie Niohrai i river, A)f omia oldiqiut ; from (r)!ik()t!i flronp) near the mouth of the liii? Sio\ix river, Moctra Sionxensi.s. F. H. JNIeelv cleserilM'd, from near Bear river, on Sulpliur Creek, Anomia coiicentrfca, CorhuUt voncentri- 00, C. e»(/e/inruitn\ C. pyrlformis^ and Melanin humerosa, now Pyriju- llfera hnmerosd; from tlu; North IMatte, TtuKicramua simpsnni ; from Ham's Fork, nortlieast of Fort liriduer, Mefampifs prisciis, now lihi/- tophuru.s pi'f.scus, Mclania n/'mpsonf.. now Goniohnsh nhnpsonl, M, nrctff, M. nltidula, now Lininam nitidnln, L. si,inilh^ L. retusta, Planorhis spectahfh's, P. iifahensis, and from near Fort liridyer, TTnio haydeni. Some of the latter .s[)(H!ies probal)ly beioni; to tlio Lower Eocene. In 18()1, Moek and Tlayden,* as before mentioned, separated the Cretaceous rooks of tiic Missouri rejjfion into five subdivisions, in ascending ovder, as follows : 1. Dakota Group, consisting of yellowish, reddish, and occasionally white sandstone, with, at places, alternations of various colored clays and beds and seams of' ipuro lijrnite ; filso siliclfled wood, and great numbers of leav- ■■* of iiie higher tyjies of dicotyledonous trees, with casts of P/irtre/Vr dakofens/s, AxinneaNioii.Gensi's^aui] Cyprina arenarea. Found at the hills back ot the town of Dakota; also extensively de- veloped in tho surrounding country in Dakula county, below the mouth of Big Sioux river, thence extending southward into northeastern Kansas and bej'ond. Fstiniated thickness, 400 feet. 2. Fort Benton Group, consisting of dark gray, laminated I'lays, sometimes alternating near the u[)per part with ^cams .nnd layers of soft gray and light colored limestone, Tnoceramns j»'ol)lematicii.s', /. tennirosh'atus, I. latus, I.fraf/ilis; Osfrea co/'ffesta, Venilin mortoni, Pholndomyn pnpyrocea, Ammonites mullani, A. percarinctus, A.res- pertinus, Scaphites warreni, S. hirnijonnis, S. ventricosns, S. vermi- formis, Nantilus elegans, etc. Extensively developed near Fort Ben- ton, on the Upper INFissouri; also along the latter from ten miles above James river to Big Sioux river, and along the eastern slope of the Rock}' Mountains as well as at the Black Hills. Estimated thickness, 800 feet. 3. Niobrara Group, consisting of lead-gray calcii'eous marl, weather- ing to a yellowish or whitish chalk}' appearance above, containing '■' Proc. Acad. Nat. Soi. Meixozoio tiiul Coiiiozoio Oeo-ogy mid J^nhtontology, 73 Inrgj; scnU's and otlior reinuiiis ol' llwhos, and nuniorons spet-imtMis of Ostn'd C(>)i(iesfn, iiiuichcd to iVaunnonts o( InovcrnmuH. Passiny; down into light yoliowisii and wliiliMli liniCHtonc, containinu great numbers of [nocerumns /u'olt/eniaficits, I. /)NCi(doi)ii/fJ/iji'fes, I. nu'culoidcs, lisli ^^calos, t'U'. Found in lI-j' bluffs along tliu MissoMri, 1)l'1o\v the (ircat Bend, to tiie vicinity of I{ig Sioux Hiver , also below theiL' on tin- lops of thu hills. Estimated thiekiiess, 200 feet. 4. Fort Pierre (iroup, eonsisting of dark beds of vt ry Ihie unctuous clay, containing much carbonaceous matter, with veins and seams of gypsum, masses of sulphuret of iron, nnd numerous small scales, fishes local, iilling depressions in the bed l)elow. Lower fossjliferous zone, containing Ain)iio)iites cnmple.i'iis, JidCHliie.t oi'atun, li. coiapressus, //( licocci'dH mortoni, II. turf "in, II. uinhilirafum, H. cochlea fn in, Ptijchocera.'i mai'toni, Fiism rinculum, Anisomf/oii horeclis, Aniauf- opiiis p(tlu(llni/onniti, rnocerniniis snbli.vcis, I. tcnniiincntus, bones of McKdsdurus liiissonrienst's, etc. Middle zone, nearly banvn of fossils. Upper part consisting of dark gray and bluish plastic clays, containing, uear the upper |)arj, ^dulilm dekdiji., Aiiiiiwnitea pldreiitd, liaculiies ocdtus, li. coni/ires.stis, Scd/ihite.s nodo.sn •■■, Dentdliaiit ;ii'dcile, Crdssa felht, eodiisi^ tiiexf/dut iiebra.scens/.s, Iituccrdiuns sdi/eiLii's, I. ncbrds- ceiisis, I. canaxciai, bones of Mosdsdiivax iHiss'uia'ieji.sis, etc. Found on Sage creek, Cheyenne river, White river aljove the Mauvaises Terres, Fort Pierre, and out to IJad Lands, down the Missouri on the high country, to Great Bend and near Bijou Hill on the ^lissouri. Estimated thickness, 700 feet. 5. Fox Hills Group, consisting of gray, ferruginous and yellowish f^Mudstone and arenaceous cl;iys, containin^ IJelenuiifelld hutOoNC, Xaii- tilus dekdyi, Aiiinioiiites pldccntd, A. lobdtus, Scdphitcs coni'diU, b. nicolletti, BdC'dites (irduditi, litisi/con bairdi, B'miis cidberfsoni, F. newberryi, Aporrhais ninericatid, P,seadobii cGinum nebrascenne, 3Idc- tra warrenana, Gardiuin .sabquadratum, ana a great number of other molluscous fossils, together with bones of 3IoHasdunis missoariensis. etc. Found at Fox Hills, near jMoreau river, near Long Lake, above Fort Pierre, along the base of Big Horn AFoi ,, ;iins, and on North and South Platte rivers. Estimated thickness, 500 feet. Ii Nebraska the sandstones of the Dakota Group rest directly upon rocks of the age of the Upper Coal Pleasures, or of Permian Age. They described from the Fort Pierre and Fox Hills Groups, at Deer Creek, near the north branch of the Platte river, Leda bisulcdtd, now Niiculdiid bisidcata, GercilUd redd, (JreneUd eleyantula. Cardium pertenue, now Protocdrdia pertenuis, TelUna nitkhda, now Jfdctra ■if 74 CrefftreouK, nitidnia ; (Vom the mouth of the Blij Horn river, Linyuln nitiiht, and from the head of Gros-VentrcH river, Ostrea [fabbonny and Cardium i'Airtum. And from the Ftjrt Union GroMp, on the Lower Fork of Powder river, ViciporuH rvi/ooh/naniin. F. H. Moek described, from Vuneonver Jind Snciji Islands, /fo.sltiia f,cnuin, rnoceyniaiis nuhi(nd(ifus, Mdotvn (fibbsana, linniiliUis inonuc/iis, H. occi'denf.afis, Ammonites complexusy var. suclensis, A. vancouvet'- ensi's, and Nautilus campbclli, W. M. Gabb* described, from Crosswicks and other |)lncc8 in TS'ew Jersey, Turriteltn (jranalicosM, Crassatelln transversa, now Eton transversa, A.rinaia siibaustratis, Ctenoides stiitarrosa, now Lima sqiiarrosa, Terebratulitia hallaua, Arta-on rretacens^ A. ovoideus, Natica infracarinata, Luvatia altispira, Oyrodes obtasivolvns, G. abbotti, Turbinopsis depressa, Architectonica abbotti, now Maryari- tella abbotti, Fascioluria slacki, Volnta delaioarensis, V. kanei, V. mucronata ; from Comanche Peak, Texas, Gtobiconcha c tt r ta ; h'om Mississippi, Oyrodes spillmani, Ostren pandifurmis ; from Alabama, Trochit.s morion i, Gryphwa thirsa; ; from New Jersey, Teredo con- torta, now Tnrnus contortns, Anatina elliptica, now Periploma dllip- tica, Venilia triyona^ now Veniella triyona, Area altirostris, Cii- culloia neylecta, now Idonearca neylecta, C. transversa, now T. trans- versa, Pecfen tenuitesta, Eudea dichotoma ; and from Tennessee, Ctenoides denticulicosta, now Lima denticulicosta. Isaac Leaf described, from Haddonfield, New Jersey, Corbula fonlkei, Dosinia haddonjleldensis, and 3Iodiola julice, now Volsella julioi. In 18G2, Gabb and Horn;J; described, from Timber Creek and Mull5';a Hill, New Jersey, L'ellepora proUJica, C, exserta, C. jmmila, Jle2)lo- celleporaria aspera, Escharinella muralis, lieptescharellina prolifera, Escharipora distans, E. abbotti, E. immersa, lieptescharipora mar- qinata, Bijfasira torta, B. disjuncta, Memhranipora abortiva, 3I.per- ampla, M.plebia, Flustrella capistrata, F. cylindrica, Reptojlustrella heteropora, Jietelea ovalis^ Fascipora americana, Spiropora calamus, Entalophora, quadranyidaris, E. conradi, Diastopora lineata, Stoma- topora reyularis, now Alecto leyularis, lleticidipora dichotoma, Cres- cis labiata, and from near Yazoo, Mississippi, Cellepora janewayi. Meek and Hayden§ described, from the Fort Benton Group, at '■'Proc. Acad. Nat. Sci. t Proo. Acatl. Nat. Sc\. X Jour. Acad. Nat. Sci., 2d ser., vol 5. i Proc. Acad. Nat. Sci. Me^oznir itiid Co'tionoic Gcoloijy and P(i1n'otitoU)(j\j, 75 Cliip|)(!Wii l\)int, l)olow Fort liciiton, on tlio Upper Missouri, Scaphitci* centn'c(mii.i, S. rcrmi/ormin, Ammonites mtillnuiinus, Nmifilus etc- (frtns, var. iiebifiscoisi.s, InocerdtuKx undahtindiiti, I. exotji/roides, f. fennirosfvdfus, Vcnih'n nn)rt <' Bost Jour. Nat Hist , vol. 7. t Pal. of California, vol. 1. -I' ■w Mi n I 76 Cretaceous, L. intciformis, Never I'ta secta, ArchitectoniGa horni, Conns horni, C. sinMiitus, now Surcula sinuata; from Tuscan Springs, Fusus averilli, Ficus cyprceoides, Amaurnpsis oviformis, Cinulia ohliqnd ; from Mount Diablo and other places, Fttsiis dfaboli, F. calif ornicus, Ilemi- fusus horni, H. remondL Tnrris claytonensis, T. varicosiata, Covdiera microittydma,, Tritonium horni, T. paHcivaricatum, T. whitncyi, Pseudoh'va volutiformis ; from INIartincz, near Benicia, Tuscan Springs, Texas flat, in Placer count}-, Clayton, Fort Tejon, Alameda county, Pence's Ranch, Contra Costa county, Rag Canon and other parts of California, Cinvlia pingins, Acfeonlna cdlifornica, Glohi- concha remondi, Cylindrites brevis^ iV/.vo j)oh'fft Cerithiopsis (t/fer- nata, ArchifecJonica veatchi, A. co(/nirr> clla veafchi, T. robnsfa, Galertis exrentricus^ now Galeroj^sis excentrr c, Spirocrypta pilevm,, Nerita canenta, Lysis di/plico^ta, Dentalinii piisilhim, D. cooper i^ D. sframineum, Emarginnla radiala, Patella traski, HelrJon circtdaris, H. dichofoma^ Bvlla Jiorni, Cylichna cos'ata, Jfegistoma striatum, Solen parallehts, now Plectosolen parallehis, Pharella alia, Corbvla primorsa, C. fraski, C. cvlfriforniis, C. horni G. parilis, An- atina tryonana, A. inceqiiilateralis, Pholadomya hrevjeri, P. nastifd, Nea'ra dolabriforniis,, 3Iactra ashbnrneri, now Cjmbophora ash- burneri, Lntraria truncat(t, Asnphis undtdafa, Gari fexfo, Tellina longa, T. remondi, T, hoffmannana, T. nionilifera, T. ovoides, T. ma'theivsoni, T. decurtata, T. quadra fa, T. aslburneri, T. par- ilis. T. horni^ T. calif arnica, Venus varians, V. veatchi, V. len- ficidaris, V. fetrahedra, 3Icretrix horni, 31. nifida, 31. longa, 31. oralis, now Cyprinopsis oralis, Dosinia elevata, D. gyrata, now Lv- cinc gyrata, T'xtensively, belongs to the plastic ehiy of the above subdivision. It is a very fine micaceous sand, with some fire-clay intermixed, and streaks of clay passing tiirough it. It is of a bluish-white color, ««,nuy in consistency when drained, but pasty when woiked u|) in vvatcr. Prof. E. D. (vope;*; descrii)ed, from New .Jov%{iy,Osteo2)y occupies a belt of the surface averaging aliout eight miles wide for at least half way through the State, This Group is the northern extension of the rotten limeslone of Mississippi and Alabama. The Ripley Group occupies a belt of the surface along the Memphis and Charleston Railroad about fifteen miles wide, but having a less average width across the State. The high ridges dividing the waters of the Tennessee and ^Mississippi rivers lie mostly within its aren. It has a thickness of 400 or 500 feet, and is mostl}' made up of stratified sands, though occasionally an interstnitified ]>ed of dark, slaty clay, 10 to 30 feet in thickness, occurs, or more frequently a sandy bed laminated with clayey leaves. The hills about Purdy, in McNairy, and about Lexington, in Henderson county, show these rocks well; but more interesting sections, on account of the fossils they contain, are found in Hardeman, near the M. & C. R. R. In 18G9, J. D. Whitney* divided the Cretaceous formation, which is found covering large areas on the west cwast, from Vancouver and the adjacent islands of San Juan Archii)elago on the north, through Washington Territory and Oregon to Southern California, as well as iso- lated patches in p]astern Oregon and in Mexico, into four groui)s, as follows: 1. The Tejon Group, the most modern member, is [)eculiar to Cali fornia. It is found most extensively develoi)ed in the vicinity of Fort Tejon and about IMartincz. From the latter locality it forms an almost continuous belt in the Coast Ranges to ^lai'sh's, fifteen miles east of Mt. Diablo, where it sinks under the San Joaquin Plain. It is also found at various points on the eastern face of the same range, as far south as New Idrca, and in Mendocino county, noai; Round Valley, the latter locality being the most northern point at which it i;-* yet known. It is the onlv coal-producing formation in California. This group contains a large and highly characteristic series of fossils, the larger part peculiar to itself, '.vhiie a considerable percentage is found extending Ijelow into the next group, and several species ^till further down into the Chico Group. Mr. Gabb considered it as lie probable equivalent of the JNIaesti'icht beds of Europe. 2. The Martinc/ Group, which includes a series of beds, of small geo graphical extent, found at Martinez and on the northern fljink ot Monte Diablo. f :■ ^■ .1 \f^ ■Pal. ofCal., vol. 2. 84 Cretaceous, L ¥ li. The Chic'o Group, one of tlio most extensive and important mem- liors of the Pacific! coast Cretaceous. It is on the horizon of eitiior tlic ui)pcr or lower chalk of Euro|)e, and probabl}' the equivalent of both. It is extensively represented in Shnsta and Butte counties, and in the toot hills of the Sierra Nevada, as far south as Folsom, occurr- ing, also, on the eastern face of the coast ranges, bordering tiic Sacra- mento valley at Martinez, and again in Orcstimba canon, in Stanislaus count}'. It includes all of the known Cretaceous of Oregon, and of the extreme northern portion of California, and is the coal-bearing forma- tion of Vancouver's Island. 4. The Shasta Group, including all below the Chico Group. It con- tains fossils seemingly representing ages, from tlic Gault to the Neo comien, inclusive, and is found principally' in the mountains west and northwest of the Sacramento valley. Two or three of its characteristic fossils have been found in the vicinity of Monte Diablo, and one of the same species has been collectGd in Washington Territory, east of I uget Sound. Few, or none, of its fossils are known to extend upward into the Chico Group. W. M, Gabb* described, from Shasta county, from Martinez, Benicia, Colusa county, Tejon, and other places in California, Phil of eufhi s foil - (itns, Belemnifes impressn.f, Ammonites jugcdis, A. sfohczknnus, A. fraternvs, Ancylocerns Uneatiim^ Diptychocerns laet^e, Fnsns tumidim, F. ore idenf alia, Ifeptvnen crefncea, JV. mucronafa, Pnlcnatrnctus crassns, Surculn piveatfe. nata, 8. inconspicua, Heteroterma trochoidea-, Bela clrithrdfn, Cordiera mifrwformis, Trifonivm colifornicum, T, tejonense, T. fusiforme, B rachysphingus sinnatus, Bullia striata. Turbinellf C7'assitesfa, Urosyca luncdnta, JSieoerita. globosa, Am.pnllina striata, Terebra calif ornica, Cyprma mathewsoni, Anchura trans- versa^ A. carivifera, Helicaulax biearinata, H. costata, Loxotrema turritd; Atresias liratiis. Tnrritella martinezensis, Nerita triangulata. Calliostoma radiatum, Ataphrtis crassus, Margaritella anyitlata, Acmwa tejonensis, Aetoionella oviform.is, Liocium pmictatum, Ringi- nella polita^ Sol en cnnetitus, Anatina quadrata, Pholadomya oregon- cnsis, Pleiiromya papyracea, Arcomya undnlata, Jfactra tenuissima, Asaphis innlticosta, Tellina vndidifera, Donax latns, Venus aequila- feralis, Jferetrix fragilis. Thetis elongata, Cardium, translucidum, Crassatella compacta, JJnio hubbardi, Modiola major, now Volsella major, Meleagrina antiqua, Tnoceramus elliotti, I. ivhitneyi, Tri- gonia aequicostata^ ITucula soli tar ia, Pecten martinezensis, P. com- plex! costa, P. interradiatus, Neithea grandicosta, Lima shastaensis, * Pal. of Cal.. vol. 2. •i Mesozoic cind Cwnozoic Geology and Palieontoloyy. sn L. multir(((linfa, Anomia vaticonverensis, Osfvca idrlaensls^O. (ippressa, RlnjHc/honeUd whifneiji, SinlJoh'orhuH vAirtus. And from tlie SiciTii de lus ('oiifluis. neiir Arivoclii, Sonora, .Mexico. Fusas mexicdiiiis, Knxplni Uihidatd, C/ieiniiitziif, .zebra, Ti/los/oiuti niutabile Anchin'ci moniliferd, CcriJhiani iiicxiranxm, Aixjdi'ld cin- yiilafa, C/nidia rertilabrnni, Pkolndoniyd nonorensis, Ciwdiiun NabulosHiii, C. ;ir(tiiul(fernm, Cardlhi alficosta, liemondia farcatn, CiicalUta inennis, Gri/phcKt miuwoimfa. Prof. E. 1). Cope* tloscribud, fVoiu Raritun bay, Oniit/iofdi'sas im- munis; from Wcslcni Kansas, Macrosdurus pt'oriijei', now Li.odon prorif/er ; from Sampson county, North Carolina, Jli/pst'benid crdssi- cduda, Jlddfosdio'i's tripos, and Po/ydecfes bifin'fjidus; from Nou' Jorsoy,f MosdsdKrits nidxiiiias, and from Alabama, Ch'ddstes propyfhon. Prof. O. C Marsh* described, from the greonsand marl, near Horners- town, IMonmonth county. New Jersey, Mosasdnrus copedniis^ M. miersi, M. princcj>s, JfdlisdnrKs/rdferinis^ now lidjjtosdxrusfraternus, and //. p/dfi/spondi/lus, now U. plttli/spondijlus. Prof. Leo Lescjuereuxj^ described, from the Daliota Group, at I'ort Ellsworth, Nebraska, Populites microphyllas, Pkyllifes belnhvfolins, Persed nebrascensis, now Laurus jiabrascensis, and Sassafrcts leconfe- anum, now Persed leconle ((lilcMt beds of tlic Hciir river coiinli'y oC l't:ih iiiul Wvoiuiiiji', properly bcloiiniuu' to tlio Tortiiiry, (tlu'V firo now regiirdc^l ms Cretjiceoiisj, niid so iutiniMti'ly rcliitt-d t(» llio hitcst C'retiicooiis, coiitMiu species of f'ot'huld, Ci/rciu/ {('orbicnln) [jorluips Octree, iunl a univalve iclateil to Me/aiiiptM, directly asso- ciated with several species of G^f^/z/o/jf/.s/.v, two of U /!>'(/, one or two of Melnnfho, several species of Vicipnms, one of Thii'ii, etc., showing' clearly -that these striitji were deposited in brackish waters. These shells also exist iu yreat numbers, and are preserved in a condition, sliowin<4' that they could not have been transpoited far by currents, l)ut that they must have lived and dieo, at least, near where wc now find them. All i)alieontologists are aware of the fact, that the remains of fresh and brackish w.ater shells do not generally present such well marked peculiarities ot form, ornamentation, etc., in beds of diirerent ages, as we see in marine t3'pes, so that they can not always l)e relied upon, with the saiue degree of coiifhlence in identifying strata, that we [)lace in marine forms; some of those from oldest Cretaceous being, for instance, very similar to existing species. So far as I have been able to com- pare the species from this formation with described forms from other parts of the world, they generally agree most nearly with Lower Eocene types; the Curhicidn and Tiani being very similar to forms found in the lower lignites of the Paris basin, and at the mouth of the Rhone in France. At the same time it is wor;thy of note, that most of these shells are quite unlike any of the known existing North American species, and one of them (Tiara humerosa) liblongs even to a genus entirely unknown among the existing Melaina of the American C(mtinent, though found inhabiting the streams of .Madagascar, the Fejee Islands, etc. One of the Uniones [iT. hellipUoatiis) resembles in its ornamentation some of the South American species, and the genus Castalia, much more nearly tiian it does any of the recent North American species, although having the form and hinge of a true U/iin: and another abundant bivalve, found in the same association, Corbula {Atusothyrin) pijriforinis, seems to be allied in some respects to a peculiar group recently described from a Pli3cene or Miocene forma- tion, on the Upper Amazon of South America, by Mi-, Gabb, under the '•' Am. Jour. Conch., vol. ti. tAdvuiu'c piunphlet from ILiyden',-* U, 8. (Tco.Sur of Wyominp:, Pte. IMAGE EVALUATION TEST TARGET (MT-3) 1.0 I.I Li §7^ |2.5 ISO ■^~ Ml^B ■^ 1^ 12.2 !^ |££ 12.0 L25 i 1.4 1.6 Photographic Sciences Corporation M \ ^\^ [V ''"-is 23 WEST MAIN STREET WEBSTER, N.Y. 14580 (716) 872-4&03 %> o^ 88 C V. aceous- i'ft w ■ % a % % name Pachijdon, and afterward renamed Anisothyris by Mr. Conrad, becanse the name Pachyodon had been previousl_y used for another genus. Of course, comparisons of the sheds, from this formation with those of the Tertiary' beds of the Atlantic and Pacific slopes, afford no aid whatever in fixing its precise position in the series, because the species from the latter are, almost without exception, marine types. There is less difficulty, however, in drawing parallels between it and the Terti- arj' deposits of the Upper Missouri country, by a comparison of fossils, although the species are mainly different, so far as jet known, in these two districts. At least two of the known forms, however, from the Utah and Wj'omingbeds under consideration, are believed to be spe- cifically identical, with species found in the oldest beds, referred to the Tertiarj^ at the mouth of the Judith river, on the upper Missouri, under the name of the Fort Unloa Group. Thesis are Unio prlscus, and Viviparus conradi. In addition to this, the fossils at these two localities are in precisely the same state ot preservation, and have a more ancient appearance than those of the later deposits of both dis- tricts, while they also agree exactly in their mixture of brackish and fresh water characters. Again, j^t both localities, these deposits are intimately associated, as already stated, with what appears to be the latest of the Cretaceous series; while in both districts they contain lignite, and are succeeded by later Tertiarj' beds of strictly fresh water origin. He described,* from the Fort Pierre Group, near the great bend in the Upper Missouri,* Isocardia hodgei, now Procardia hodgei. Prof. O. C. Marshf named, from the Niobrara Group, on the North Fork of the Smoky river in Kansas, Edestosaurus dispar, now Cli- dasfes dispar, E. velox. now C. viz:., Clidastes pumilis, C. wgniani, and Pterodactylus oweni.^ Prof. E. D. Cope described,.§ from the Niobrara Group, near Fossil Spring canon, Edestosaurus stenops, now Clidastes stenops, E. tortor, now C tortor, Ilolcodus coryphams, now Platecarpus coryphoius, Liodon curtirostris, now P. curtirostris, L. glandiferns, now P. glan- diferns, Portheus molossus, P. angulatus, now Erisickthe angulatus ; from Butte creek, Holcodus tectubis, now Platecarpus tectulus, Pro- tostega gigas ; and from one mile southwest of Sheridan, near the Gypsum Buttes, TAodon latispinus, now Platecarpus latispinus. " Proc. Acad. Nat. Sci. t Am. Jour. Sci. and Arts, 3d series, vol. 1. X Proc. Acad. Nat. Sci. Mesozoic and Coenozoic Geology and rahvontoloyy. 89 In 1872, Prof. E. \V. Hilgard* showed that the Cretaceous of Alabama and Mississippi has a dip sensil)ly at right angles to tlie trend [i.e., between W. and S.) at the rate of 20 to 25 feet per mile. That the lower division, called the Cotfee Group, or the Eutaw Group is from 300 to 400 feet thick, and consists of noncalcareous sands, and blue or reddish laminated clan's, with occasional beds of lignite, and rarely marine fossils, silicified, as at Finch's Ferry in Alabanm. This group corresponds with Hayden's Dakota Group, and in its upper part, as at Finch's Ferry, probably with the Fort Benton Group. The Middle or Rotten Limestone Group is nob less than 1,200 feet in maximum thickness, consisting of soft, mostly somewhat clayey, whit- ish, micro-crystalline limestones, and calcareous clays; very uniform on the whole, with the exception of the locally important feature of the "Torabigbee Sand." The Cretaceous area of Arkansas, according to Owen's description, seems to fall witliia this group, as does also the greater part of the Cretaceous area of middle and northern Texas. The Ripley Group consists of crystalline, sand}' limestones, alter- nating with dark-colored ^lauconitic marls, containing finely preserved fossils, and has a thickness of 300 to 350 feet. It is the equivalent of the highest Cretaceous beds of New Jersey, and of the Fox Hills Group of the West. The series of isolated Cretaceous outliers, which traverse Louisiana, from the head of Lake Bisteneau, in a S. 8. E. direction to the great salt mass at Petite Ansc, belong to this Group. Prof. F. V. Haydenf said, that in Nebraska, tho sandstones of the Da- kota Group rest directly upon rocks of the age of the Coal Pleasures. Al- though they do not appear in full force until we reach a point near De Soto and beyond, yet remnants of the sandstones make their appear- ance within five or ten miles of Omaha, at any point north of the Platte river. It is quite probable that they once extended all over Nebraska, passing across into Iowa, and further eastward. The Coal-measure limestones are thus exposed, in northeastern Nebraska, b}' the erosion of the Cretaceous rocks. Near the entrance of the Big Sioux river,- into the Missouri, the Dakota Group disappears beneath the water-level, and is succeeded by a series of black, plastic, laminated clays, with lighter colored arenaceous part- ings and thin layers of sandstone. Near the mouth of the Vermilion river the upper portion becomes more calcareous, and gradually passes up into the next group, called the Fort lienton Group. It is often immensely thickened, in the vicinity of the mountains, from the north I I 'I 1/ I, * Proe. Am. As.«. Ad. Sei. t Hiiyden's U. S. Geo. Sur of Wyoniiner. ^'' 90 Cretuceons. 'liii I' lis!' ti;.'' Jji'.i m :; 1 fS!" line to New Mexico, but on the Lower Missouri, where it was first ob- served by geologists, it never reaches a thickness of more thiin 150 or 2U0 feet. In New INIexico it occurs us the most conspicuous of the Cretaceous divisions, and along the line of the Kansas Pacific Railway, in Kansas, it has yielded large quantities of the most remarkable rep- tilian remains. The Niobrara Group in found, in some form, wherever the Cretaceous beds occur, from the north line to New 3Iexico, a.nd probably much farther. As it is developed on the Lower Missouri, and southward through Nebraska, Kansas, into Texas and the Indian Territory, it contains thick, massive beds of chalky limestone. On the Kansas Pacific Railway, at Forts Hays and Wallace, this limestone is sawed into blocks oC any desirable size, with a common saw, and used for building purposes; but along the flanks of the mountains, or in the far west, it never reveals its chalk}' character. It is found in thin, slaty, calcareous layers, but universally characterized by the presence of the oyster Osfrea congesta, and also ^ome form of Inoceramiis, or a few fish remains, but the little oyster is ubiquitous. In these three divisions there seems to be no well-marked line of separation, and the more we study them the more intimately do they seem to be blended together. The Fort Pierre Group begins to overlap the Niobrara Group below the mouth of the Niobrara, and above that point, although the river cuts deep down into the chalk limestone, and long lines of cone- like blulfs extend up nearly' to the Great Bend, yet the distant hills on either side of the river show plainly the dark shaly clays of this group. This ^roup covers a vast area of country, perhaps 5,000 S(iuare miles or more, and wherever it prevails. It gives to the sur- face the aspect of desolation. The entire thickness of the group is filled with the alkaline material, which is so well known in the west, and wherever the water accumulates in little depressions and evap- orates, the surface is covered with a deposit of the salt varying from an inch to several inches in thickness. The water that flows through these clays is usually impregnated with these salts and thus rendered unfit for use. Although these claj's seem to be so sterile, and in the diy season are typical of extreme aridity, ^-et they are i)y no means destitute of vegetation. The various species ot chenopodiaceons shrubs and herbs, that are peculiar to the west, find their natural habitat in these clays, and grow most luxuriantly. The Sarrohatns reaches its highest growth in this region. The somber appearance given to the country by the black cla^'s is unfavorable to it. At the Great Bend m m Jlesozoic and Crenozoic Geology and PaJn;onf,oJo(/if. 91 there is a large thickness of the strata filled with concretions that are made u]) nio>itly of an agu;r(\<>ate of fossils, as Ammonites. Bncv- lites, etc. Near Ciiain de Roche creek these concretions have been swept down into the Missouri by the swift curre it, during the spring floods, and in the low water of autumn they present a picturesque appearance. Although the rivers cut deep channels through the different forma- tions, we do not meet with the Fox Hills Group along the Missouri, until we reaoh nearly up to the mouth of Cannon Ball river, yet fifty miles or more before reaching that jjoint it has overlapped the Fort Pierre Group. In titiveling across the plnin country westward from Fort Pierre,, we find it occupying the entire area. Very soon after pass- inund ferruginous concretions, and numerous beds, seams and local deposits of lignite, great numbers of dicotyledonous leaves, stems, etc, of the genera Plnfanus, Acer, Ufmus, Popiilns, etc., with very large leaves of true fan palms; also Helix, Melania, Vit'ipard, Corbicida, Unio, Osfrea, Corhula and scales oi' Lepidotus. with l)ones of Trion/x, Emjjs, Compsemys, Crocodihis, etc; as occupying the whole country around Fort Union, extending north into the British possessions to unknown distances, southward to Fort Clark, under the White River Group on North Platte river above Fore Laramie, aiidon the west side of Wind River mountains ; and as having a thickness of 2,000 feet or more. The passage from the brackish to the fresh water beds seems not to be marked by any material alteration, in the natnni of the sediments; nor have we any reason for believing, ihat any climatic or other important physical changes beyond the slow rising of the land, and the conse- Proe. Aea appeared. In the sandstone, marine life still marks its activity onl}- by the abundant remains of fucoids, indicating, by their growth, a com- paratively shallow water. They point out, therefore, a slow upheaval of the bottom of the sea in which they appear to have lived; for their stems penetrate the sandstone in every direction. And this indication is still more manifest in the great abundance of debris of land-plants. • I 100 Cretaceous. .(,( i •I J' i ; 1 I .1 pi !l. i wl wliicli seem as if ground by the waves, thrown upon the shore and mixed in the sand with fucoidal remains. Tiiat this sj* idstone forms all over and around the Raton mountains, the oase of what is called the Lignitic Group, and that it overlies the 1)lack shale of the Fort Pierre Group, has been remarked by all tlie geologists who have explored the country. Dr. Lecontc, considering tiie strata as Crelaceons, mentions them in his report as continuing southward of the Raton, along *!ie liase of the Rocky mountains, forming -"u immense terrace, wl.ieh extends as far south as the valley of the Tonejo, and perhaps even to the north bank of the Cimarron. From this place northward to the base of the Spanish Peak, these sandstone beds, always with !,he same characters and superimposed upon the Fort Pierre Group, form an im- mense terrace, perpendicularly cut, like a wall facing east, high above the plain. They support the lignitic beds which still tower above them, either ascending in steep declivities from the top of the perpen- dicular sandstone, or receding at some distance, where they have been more deeply sapped by erosion. Tnis abrupt front, says Dr. Hayden, seems to form a sort of shore-line of a wonderful basin, as if a body of water had swept along and washed against the high bluffs, as along some large river. The stage-road from Trinidad to Pueblo follows .the base of these cliffs for thirtj'-two miles. South of Trinidad, the lignitic measures have been followed nearly without interruption to the Maxwell estate, about fifty miles. The area which they cover, at and around the Raton mountains, may be estimated : t 600 to 800 square miles. The same formation is reported farther south, near and around Santa Fe; in the Gallisteo valley; along the mountains to Albuquerque, and in the valley of the Rio Grande, as far south as Fort Craig. Everywhere, with a single exception, these Lignitic measures have exposed, hy their relative position, by the absence of animal remains in the thick beds of sandstone, which indicate their base and constitute their foundation, by the homology of their marine and land flora, as recognized in the remains of fossil-plants Avhich they contain in abundance, all the characters authorizing the separa- tion of this group from the Cretaceous formation. From Pueblo to Canon City, fortj^-five miles, the stage-road follows a broad valley-, closed on the south side by the Greenhorn mountains on the north side by the Rim Range of the Colorado mountains, over which towers Pike's Peak, whose summit is visible all the time. The whole valley is essentially Cretaceous; all the eminences, either near the borders or in the middle, are hills of this formation, molded by the erosions of the Arkansas river, which has dug numerous beds in this if Mesozoic and Camozoic Geology and Pala'outology. 101 soft material. The borders of its [present bed, like those of its old ones, where the road sometimes meanders, as in a labyrinth, arc pic- turesquely marked by rocks of diversified forms, resembling monu- ments built by the hand of man, towers, columns, ruins, etc., often strovvn around in confusion. On the south side of the river, however, about fifteen miles before reaching Canon City, the aspect of the country is modified by the appearance of a group of hills of the Lig- nitic, filling the space from the base of the Greenhorn mountains to the borders of the river, three to four miles in width. The whole area covered here by the Lignitic is about 3.3 square miles. The lower strata, overlying the sandstone, rise abruptl}^ about 50 feet above the Arkansas river, forming a kind of narrow plateau, over which the hills of the upper Lignitic rise up to about 500 feet. The whole thickness of the lignite bearing strata is estimated at about 600 feet. The lower sandrock, about 200 feet thick, is the equivalent of the lower fucoidal sandstone of the Lignitic of the Rat'n mountains, and it graduates into the Lignitic above. Indeed, in some places the lower sandstone includes in its divisions beds of lignite to its ha^e. From Pueblo northward no trace of the Lignitic is seen along the mountains till near the southern base of a range of hills, the Colorado pinery, which, in its eastern course, at right angles from the primitive mountains, forms the divide of the waters between the Arkansas and the Platte rivers. The succession of the Cretaceous strata is clearly marked on the banks of Monument creek. In following it up from Colorado Springs, the formation can be studied to the top of the black shale of the Fort Pierre Group, and above this to a bed of brownish sandstone, separated from the black shale by thin layers of Tuten clay and soapstone, where tlie last remains of Cretaceous animals, especially frasments of liacnlites, are still abundant. Over this is the sand- stone, barren of any kind of remains, overlaid in the banks of the creek, by a bed of fire-clay, or very soft chocolate-colored shale, which marks the base of the following section at low-water level of the creek : 1. Brown, laminated fire-clay, or chocolate-colored soft shale, a compound of remains of rootlets, and leaves and branches of unde- terminable conifers, 2 feet. 2. Coal, soft, disaggregating under atmospheric influence, 2 feet. 3. Chocolate-colored clay shale, like No. 1, with a still greater proportion of vegetable debris, 6 feet. 4. Soft, yellowish, coarse sandstone in bank, 8 feet. I, i 102 Cretaceous. \\ i' It ('\ I 5. Cluy, shale and shal}' sandstone covered slope, 130 feet. 6. Soft, laminated clay, interlaid by bands of limonite iron, thin lignite seams, and fossil-wood, 88 feet. 7. Lignitic black clay, in banks, 32 feet. 8. Fine-grained conglomerate, 112 feet. 9. Fine-grained sandstone, 4 feet. 10. Coarse conglomei'ate, 7 feet. 11. Sandstone, 3 feet. 12. Ferruginous hard conglomorate, 32 feet. Total, 426 feet. The soft chocolate-colored, laminated clay, Nos. 1 and 3 of this sec- tion, has the same composition, color, and characters as the clay under and above the coal-beds of the Raton mountains and of the Arkansas valley. It is the same, more or less darkly colored by bitumen, which prevails over the whole area of the Llgnitic. ' This day takes the place of the fire-clay so generally' underlying the coal-beds of the car- boniferous measures, where, as in the Lignitic, it forms, beside the floor, some bands, clay partings, separating cool strata, and soft shale overlying them. The dicotyledonous leaves, specifically identical with those found at Raton mountain and in the Arkansas valley, 1.?ave no doubt about the cotemporanelty of these Lignitic measures. B}' far the most interesting member of this section is the conglomer- ate at the top. This is a compound of small grain'* or pebbles, mostly of white quartz, and ofsilex of various colors, varying in size, at least for the largest proportion, from that of a pea to that of the head of a pin. Pebbles as large as a walnut are abundant. This formation. 150 feet thick, at least, is conformable to the strata overlying the coal of the base of the section, and here, as it Avill be seen at other places, it over- lies immediately thick banks of soft, laminated, bituminous, bl.ick clay. The materials forming this conglomerate are cemented together by a thin coating of carbonate of lime, which easily disaggregates under at- mospheric influence, except in the upper stratum, where the cement has beeii hardened bj^ ferruginous infiltration. Its greater resistance has then locally preserved the whole mass from destruction. These conglomerate cliff's, which, from the hotel of Colorado springs, arrest the view to the west, appearing like high blufts of white sandstone, are evidently the mere vestiges of an extensive formation, originally cover- ing the base of the mountains from the Arkansas river, extending' far inland to the east. For hundreds of miles the ground of Colorado is formed by its debris. They have given to the soil, that apparent sterility of surface, which is so remarkably changed into fertility, by the culture Mesozoic and Ccenozoic Geology and Palceonfolof/y. 103 of the substratum composed of softer-grained materials and lime. Nearer to and along the base of the Colorado pinery, whose lignitic hills have escaped destruction, by the upheaval of the ridge, these cour glomerates, still detached from the common mass, and molded into the most diversified forn.s by disintegration, have scattered columns, pin- nacles, round towers, and cupolas over a wide area, the far-famed Monument l*ark. From the mouth of Bear creek into the Platte, a few miles west of Denver, the Lignitic formation abutting against the Cretaceous and diversely thrown up b}' the upheaval of the primitive mountains, fol- lows the base of these mountains in a nearly continuous belt to Chey- enne. Though generally covered by detritus, the basin is deeply cut by all the creeks descending to the plain — Clear, Ralston, Coal, Erie, Boulder, Thompson g_v, we find, in its abrupt and permanent separation from the Cretaceous, its lithological com- pounds, its total barrenness from animal remains, at least generallj*, and the homogeneity of its flora, reliable and constant characters better defined than in an}' geological division admitted by science. This sandstone formation is inexplicable. It can be compared to nothing but the millstone-grit of the Carboniferous epoch. How to explain why, at once, animal life seems to disappear from the bottom of the sea, to be superseded by marine vegetation? May this change have been caused, perhaps, by a rapid increase of temperature (esozoic and Cainozoic Geology and Paloiontology. 107 of the water brought up b}' the force acting to the upraising of the bottom into land, and afterward into chains of mountains. Tiiough it may be, this change is evident and proves the geological discrimina- tion of the Eocene sandstone from the Cretaceous, a separation the more remarkable, that from numerous observations this sandstone is i-eported constantly conformable to the Upper Cretaceous beds. As Dr. Ha^'den remarks in his description of the Lignitic Group of Nebraska, when we bear in mind the fact that wherever tliis forma- tion has been seen in contact witii the latest Cretaceous beds, the two have been found to be conformable, however great the upheavals and distortions may be, while at the junction there seems to be a complete mingling of sediments, one is strongly impressed with the probability that no important member of cither system is wanting between them. After contrasting the distribution and character of tiio plants with those known from the Tertiary of other parts of the world. Prof. Les- quereux thought himself authorized to deduce the conclusion: That the great Lignitic Group must be considered as a whole and well characterized formation, limited at its base by the fucoidal sand- stone, at its top by the conglomerate beds; that. Independent from the Cretaceous under it, and from the Miocene above it, our Lignitic f o - mations represent the American Eocene. He described, from South Park, near Costello's ranch, Ophioglossum nlleni, now Salviaia alleni, Planera long/folia; from Elko station, Nevada, Sequoia angusfffolia, Thujti garmdnl, Abies nevadensis; from the Raton mountains, Sphairia lapidea^ Chondrites subsimplex, C. bul- bosiis, Halgmenifes major, IT.striatns, Delesseria iiicrasscta,. now Cau- lerpifes incrassatns, Delesseria lingulata; from Gohiung's coal-bed, near Colorado Springs, 7)om6e//o/),v/« o6^<6s'r<; from Golden Cit}-, Col- orado, Sclerotium rubelliun, Delesseria ffdva, Pteris anceps, Carex berthoudi^ Sabal goldana, Qaercus stramiueus, Ulmus irregularis, novf Ficus irregularis, Ficus auriculata, F. spectabilis, Cissus kvvigatus, Dombey apsis trivialis, D, occidenialis, now Ficus occidenfalis, Sapindus cavdatus, Cennothifs^/ibrillosKs, now Zizyphus Jfbrillosus, Rhamnus cle- burni, B. golda,ins, R. goldanus, var, lafior; from Erie Mines, Boulder Valle}', Canlinites fecnndus, Cerris eocenica; from Carbon station, Wyoming, Populus decipiens, Ficus obhinceolata, Coccolobn Imvigata, Asimina eocenica, Zizyphus meeki; from Black Butte station, Sphaeria myrica:, Opegrapha antiqua, CauUnites sparganioides, Myrica torreyi, Ficus planicostata, F. lilanicostata, var. latifolia^ F. clinfoni, F. cory-. lifoUus, F. haydeni, Vibernum marginatum, V. contortum, Cissus lobato crenatus, Aleiirites eocenica, Paliurus zizyphoides, Carpolithes r *■ 108 Cretaceous, falcatus; from the Black Butte saurian berl, Vihernum diehotomum; from the Black Butte red baked shale, Qitercn.s wyominyanus; from Evanston, Calycites hexaphylla, Carpolithcs arachioides, now Leynm- inosites arachioides; from Elk creek, near Yellowstone river, C<(rpo- lithes osseins; from six miles above Spring canon, near Fort Ellis, Abies setigera and Nyssa Lanceolata. He described, from the Dakota Group, six miles south of Fort Harker, Kansas, Jlymenophyllum cretaceiun, Caulinites spinosus, Populites fagifoliu, t'iciis sternhergi, now Persea sternbergi, Sassa- fras mirabile, S. recurvatum, now Platanus recurvata, 8. harker- anum, now Cissites harkeranns, LairrophyllHrn reticulatum, Pteros- permites sfernbergi, now Protophyllnm sfernbergi; from nine miles above Salina in tjie Saline Valley, Kansas, Populites saJinoi, now Men- ispermites salinensis, P. ajffinis, now Cissites affinis, and Pterospermites rugosvs, now Protophyllum rngosum. Prof Meek* said that the coal-bearing rocks at Coalville, Utah, are undoubtedly of Cretaceous age, as he had from the first maintained, and he quoted in support of this view his remarks in Dr. Hayden's Report of 1870, page 299. He prepared a section running from the principal coal-bed, near Coalville, in a northwesterly direction, to Echo canon, a distance, b}' a right line a little obliquely across the strike of the roi ks, of about three and a half miles. This section commences 393 feet below the heavy bed of coal, and furnishes a thickness of 3,980 feet below the conglomerate, or including the conglomerate, which is here 700 feet in thickness, 4,680 feet of strata. Several parts of this section contain marine Cretaceous fossils, the highest of- which is gray, soft, sandstone, 30 feet in thickness, and 1,431 feet below the con- glomerate. It contains many large Inoceramus, Ostrea and Cardium^ The conglomerate not only composes the towering walls of Echo canon at places forming perpendicular, or even overhanging escarp- ments,. 500 to 800 feet in height, but also rises into mountain masses on the west side of Weber river, near the mouth of the canon. It probably attains a thickness in places of 2,000 feet. This he referred to Tertiary age because of its position above the Cretaceous, its non- conformability with the rocks below it, and its remarkably coarse material. *6th Rep. Hayden's U. S. Geo. Sur. Terr. Menozoic and Camozoir Qrology and PolcBontoJogy, 109 Keciirrln<5 to the Rocks at Coalville, ho says: As I have, however, mentioned CaultH and lateral displacements of the strata )\ere, it may be thought, by some, who are yet incredulous in regard to theCretace- <)us age of these coals, that these disturbances of the strata may liave 4jiven origin to erroneous conclusions respecting the position of the beds containing the Cretaceous types with relation to the coals. This, however, is simply impossible, because these fossils occur both above and below the coal beds, even in local exposures, where all the strata, and included coal-beds can be clearly seen conformable and in 1 heir natural jwsitions with relatior to euch other. We found both above and below the main coal-bed, Inoccrainus 2)ro&^em« /;«,<», a widely distributed species, tliat is very characteristic of the Niobrara and Benton Groups of the Upper Missouri, which there occup}' positions below the middle of the series. Again, far above this, numerous speci- mens of a larger Inoceramus, which, if not rcall}' identical with one of these forms, is scarcely distinguishable from /. sagensis and T. nehras- i'ensis. which occur in the later members of the Upper Missouri series. From these facts, it is more probable that we have here, at and near Coalville, representatives of the whole Upper Missouri series, with'pos- sibly even lower members, farther up Weber river, than any of the known Upper Missouri subdivisions of the Cretaceous. If this is so — and there seems to be but little reason to doubt it — the marked differ- ence observed between almost the whole group of fossils found here, and those of the Upper' jMissouri Cretaceous, would seem to indicate, that there was no direct communication between the Cretaceous seas or gulfs of that region and those in which these Utah beds were de- posited. Differences of physical conditions, however, probably also played an important part in the production of this diversity of life, since it is evident from the great predominance of clays and other fine materials in the Cretaceous beds of the Upper Missouri, that they were deposited in comparatively deeper and more quiet waters than those in Utah, in which coarse sandstones, with occasional pebbly beds, predominate. The strata including the beds of coal exposed on Sulphur creek, J no Cretaceous. • i near Bear river, In WcMtern Wyoniing, he roj^arded us of the same a<,'c as the CoalviUe series. His seetion liere is 3,542 feet thiek. Tlie lower 1,21.1 feet he regarded n.r, certainly Cretaceons, tlie next 2,049 feet he tliouglit is probably Cretaceons, and the npper 280 feet he regariU'd as of Tertiary age. Tiie IJitter creek series, wiiich is found along liittcr creek (a small tributary of Green river, in Wyoming), from Black Butte northwest- ward to Snlt Wells Station, on the i'nion Pacific Railroad, and at Rock S[)ring, and some other [joints west of Salt Wells, consisting of a vast succession of rather soft, light-yellowish, lead-gre}-, and whitish sandstones, with seams and bods of vaiious colored clays, shale, and good coal, the whole attaining an aggregate thick- ness of more than 4,000 feet, [)res(M>t a mingling of fresh, brackish, and salt water types of invertebrate fossils, such as Goniobasis, Vivlparus, Corhi'cuUt, Corbii/a, Osfrea, Anomltt, and Modiola. This is the Lig- nitic Group which Prof. Lesqucreux determined from the charaeter of the plants to be of Kocene age, and Prof. Cope, from the Dinosaurian remains, to be of Cretaceous age. Prof. Meek thought the Judith river brackish-Avater beds are of the same age, and that the inverte- brate fossils alone left tlio question of the age of the series in doubt. He stated the information as to its age in the following summary: 1. That it is conformable to an extensive fresh -water Tertiary for- mation above, from which it does not differ materiallv in litholo<>ical characters, excepting in containing numerous beds and seams of coal. 2. Tliat it seems also to be conformable to a somewhat differently composed group of strata (1,000 feet or possibly much more in thick- ness) below, apparentl3' containing little if an}' coal, and believed to be of Cretaceous age. 3. That it shows no essential difference of lithological characters from the Cretaceous coal-bearing rocks at Bear river and Coalville. 4. That its entire group of vegetable vemains (as determined by Prof. Lesquereux) presents exclusivelj' and decidedly Tertiary af- finities, excepting one peculiar marine plant [Hnlymeniles)^ which also occurs thousands of feet beneath undoubted Cretaceous fossils, at Coalville, Utah. 5. That all of its animal remains, yet known, arc specifically different from anj' of those hitherto found in any of the other formations of this region, or, with perhaps two, or possibly three exceptions, elsewhere. 6. That all of its known invertebrate remains are mollusks, con- sisting of about thirteen species and varieties of marine, brackish and I i Mcsoznlc (n\(I (Urnoznir (ieohx/n mid PiiUvonhthufy, 111 fresh wat(M' typcn, none of whitli bi'lonjj to jjfencni pci'iilinr to tlio Crctnceons or iiny older rocks, l)ut nil to sucli us are alike coimiioii to the CretuceoiiH, Tertijiry .'iiul present epochs, witli possildy the excep- tion of frouiobonin, wliidi is not yet eertiiinly known from the Cretiu'ooiis. 7. Thiit, on the one hiind, two or three of its species 'nelonfj; to sections or siil);;ener!i ( L(:j)f(:tisiform.is, Admefe rhom- boides, A. siibfiisiformis, Ttirritella coalvillensis^ T. micronema, T. spironema, Fiisas (jubbi, F. iitahcnsh, Turbonilla codhuilersi.s, En- linia chrysalis, E. inconspican, Jfelampus antiqtnis, Vahafa natni. P/i//sa oarZei'oxi; from the Missouri river below Gallatin City, ^Montana, Ostrea anomioides, Corbicida injiexa, Pharella pealei ; from Bear river city, on Sulphur crejk, Wyoming, Trapezium micronema, Corbi- cida wqiiilateralis, C. secvris, from near Cedar City, Southern Utah, Corbula nematophora; from the Bitter creek series, at Point of Rocks, W^'oming, Ostrea wyomingensis, Corbula tropidophora; from Black Butte Station, Corbicula banmst.eri, Melania vyomingensis; and from Rock Spring Station, Central Pacific Railroad, Wjom- ing, Corbula vndifera and Goniobasis insculpfa. IPZ Ci'cfftceoiiir. Prof. E. D. C,\)|)c''' (loscribcd, from Solomon river, FxansftH, Portheuif gladius, now Peleroptcrus glndiuit, aiu\ Porfhetis lesfrio. Prof. O. C. Marnlif doscnlxid, from Kunsiis, ApntorniH celer. F)r. Joseph LeUly* lU'Hcriix'd, from Smokj Hill river, Kjiiihus, Cli- dasfes ajfflniit; luul from (Joliimhus, IMississippi, IJumylodus tnqueftfns. Mr. JiimoH Riclmrdson^ separated the (/retaceous* rocks of Vancou- ver Island into seven divisions in ascending order as follows: A. Prodn(!tive coal measures. B. Lower shales. C. Lower conglomerate. D. Middle shales. E. Middle conglomerate. F. Upper shales. G. t'pper conglomerate. A section of division A., on Brown's river, is shown to be TIVJ.J feet thick. Division B., on Sable river and Denman Island, 1,000 feet. Division C, on Denman and Hornby Islands, between 900 and 1,000 feet. Division D, on Hornby Island, 70 feet. Division E., on Hornby Island, from 1,100 to 1,200 feet. Division F., near Tribune Bay, 776A feet. And Division G., on Tribune Bay. 'J20 feet. Making a total thickness of 5,000 feet. Dr. Dawson II described, from the Lower Cretaceous of Queen Charlotte Islands, Cycadeocarpxis colamhiamis. In 1874, Dr. F. V. Hayden^ said, that to one who has carefully stud- led the divisions along the ^Ilssouri river, the Cretaceous beds in Colo- rado and New Mexico, may be separated into five groups, without much difficulty. The Dakota group Is well shown and Is alwaj's char- acteristic, though seldom containing any organic remains. The Niobrara group Is represented by a thin bed of Impure gray limestone, and thin calcareous shale, wltli Osfreit congesta and a species of Inoceramus. The fossils are about the same as those occurring on the Missouri, ])ut the rocks have little of the chalky texture, as observed In the northwest and in Kansas. The Fort Benton and Fort Pierre groups are black shaly clays, and do not differ materially from the same groups occurr- " Proc. Acad. Nat. Sci. t Am. Jour. Sei. and Arts, 3d series, vol. 5. i Cont. to Extinct Vert. Fauna. W. Terr. §Geo. Sur. Can. II Geo. Sur. Can. H Ann. Rep. U. S. Geo. Snr. Terr. MeaoziHC and. Camozoic Oc(tlo{fy and Pnloionfologff. 1 1 :( iii^ in other IcK'ttlitios to tlio iiortliwiiid. 'V\\v Fox Hills j^roiip coiitiiinH n ^I'oat ui)ini(liiiK'u of well iitiuktMl Cietaccotts fosHiln, tniiiiy of tlu> Hpe- ii|) piissos tip into Iho li}j;iiito stnitu, uppari'iilly, without any nmrkiMl iiiicoiit'orni- jihility. In ptissinji; n|)wai(l in the Fox Hills Gronp, one by one the inol- InscM of purely marine eharaeter disappear until only soini; varieties of oysters remain, with tim plants pi-euliar to the Lij^nitie fJrou[). Th(! relation of the well-defined (-retaeeous with the Linnitic G uup forms one of the most important problems in Western <;eolojjf\, and the area for the solution of the tpiestion i)r()l)al)ly lies in the Laramie l)lainH and wcsstward toward Salt Tiake, where the a;,'j;rej5ate thieUness is from 10,000 to 20,000 feet. So far, the evidence from the vegetable remains is wholly in favor of the Tertiary ag<( of the coal j^roup. The vertebrate remains, aecordinjj^ to.l'rof. (!ope, pla«e tho coal jjfroup with the Cretaeeouu, while the proof from the invertebiate fossils is not strong in any direction, although, perhaps, leaning toward the Terti- ary. We must admit, however, that the lower coal-beds are of Cretaceous age so far as the evidence goes. For instance, the Coalville and Bear river bods are most probably ('retaeeous, inasmuch as many undoubted Cretaceous types are found in strata above the coal, and further south, in New Mexico, Arizona, and Utah, there arc coal-beds of undoubted Cretaceous age. A. R. Marvine* described the Dakota Group between the Big Thompson and South Platte. It can be traced from one point to the other, though it is somewhat obscured near Golden City ; this is due to the fact, that its hardness is greater tlmn the beds either above or below, and it forms a more persistent hog-back ridge than any other group. Between the cross-cutting streams for all this distance and beyond, it rises in its long characteristic ridge, capping the soft Juras- sic beds below, and whether the dip be high or low, usually reaching to about the same level. The sandstones are usually clear, gritty, eveu- grained and silicious in texture, varying from a silicious conglomerate, on the one hand, to a hard quartzite on the other, and only occasion- ally becoming soft. Their color is usually light 3'ellow or light gray, or even white, varying to rusty yellow, and only occasionally red in the softer portions. These are the hard and massive portions which characterize the group, and which are separated b}^ thin, shal}' layers, which maj"^ be quite argillaceous or even carbonaceous in character, with many broken remains of fossil plants. A section at Bear Canon <■ Hajden'8 U. S. Geo. Sur. Terr. 114 Crefdceoufi. I' W! shows a thickness of 240 feet, and another near the South Platte river, 385 feet. The Fort Benton Group consists of a series of shuly beds, wliich may be either higlily argillnccous or quite arenaceous in cliaracter, there boinjj^ associated witli them, in either case, a few th?n, brown sand- stones; the thickness from Big Thompson to South Platte var^ying from 100 to 400 feet, A section at Little Thompson creek shows a thickness of 400 feet, and one at Bear Canon 120 feet. Tlie Niobrara Group is decided!}' calcaix-ous, and usually contJiins numerous fossils. A section at Bear Canon shows 105 feet, and one at Little Thompson creek 150 feet. The Fort Piei-re Group, at Bear creek is about 300 feet in thickness. The total thickness of the Dakota, Fort Benton, Niobrara, Fort Pierre, and Fox Hills Group, at the jNIiddle Park, is estimated at from .'5,500 to 4,500 feet. A section of the Lignitic Group at Golden Cit^' shows a thickness of .3,, 300 feet, and the estimated thickness at ^Middle Park is 5,500 feet. Pr'*". LeoLesquereux* described, from the Lignitic Group at Golden Co\ova(\o,Woodwa7'dia lafilobct, Pleris erase, P. Nnbsimple,>\ P. nffinis, now Osminida nffinis, AspidliDit gohllanum, now Lnsfren (johhina, Sphenopt.eris membrnnacea, Selar/inclla berthotuli, Jii/me^opl/i/lhini covfasum., Flabellaria friicfifera, now Sabalifes fn(cfi/erns, Querriis (johlnnns, Pirns 2)l08C(l on Groon Hvcr, about two* and a half miles above Flaming Gorge; along the northern flanks of the Uinta mountains; in the Pink cliffs; at Gunnison's Butte, on Green river south of Gray canon, but especially in the eliffs and es- carped hills of the Salt Wells basin, east of the debouchure of the Point of Rocks (!anon. The Point of Rocks Group consists of sandstones, usually indur- ated, sometimes ferruginous, with many beds of carbonaceous shales and lignitic coal, and is divided into the Golden Wall Sandstone, the Middle Hogback Sandstone, and the Upper Hogback Sandstone. The rocks are well exposed at Point of Rocks Station on the Union Pacific Railroad, in the escarpments facing Bitter Creek, at Rock Springs, on Green river, 2 miles above Flaming Gorge, at the foot of Desola- tion Canon, and Gray Canon on Green river, in the Wahsatch Cliffs at the head of the P^scalante river, and in the hills at the foot of the Pink Cliff's in Southern Utah. Prof. C. A.White* described, from the Point of Rocks Group, near Point of Rocks, Wyoming, Ostrca insecir/'a, Odo.Jobasis hnccivoidea ; from Upper Kanab, Utah, ITnio (jonionotvs, FU.norhis kanabensis, Physa Icnnribenais^ Helix kannbensis ; and from Bear River Valley, near Mellis Station, Wyoming, Jthytophnrus meeki, Goniobasis cle- burni, G. chrysaloitfi punyuitchensis; from the Salt Wells Group, near Coalville, Utah, Osfrea sannionis, Area coahu'Uensis, Lxinatin lUahensis; from Last Chance creek. Southern Utah, Inocera- mus (jilbertl; and from Upper Kanab, Utah, and Hilliard Station, Wyoming, Cyrena erecta. He described, from the Sulphur Creek Group at Upper Kanab, Utah, Turnns spheiioideus, Anchnra rinda, and A. prolabiata. He described from the Henry's Fork Group at the head of Water- pocket canon. Southern Utah, Plicntula hydrotheca; from Lower Potato Valley and Upper Pine creek, Utah, Inoceramus howelli; from Middle Park, south of Grand river, Colorado, Avicula parkensfs. He described, from the Bitter Creek Group at Black Buttes,W3'oming, Unio jjetrinus, XT. prupheticiis, U. brachyopisthns, Neritina volvi- linenta, Viviparus plicapresfms. Leioplax tiirricida; from Almy coal mines, near Evanston, Pisldium saginatnm, Hydrobia recta; from Point of Rocks, Corbvla subandifera; from south base of Pine Valley Mountain-., Utah, Helix peripheria, and from Musinia plateau, Hydrobia utahensis. '•' Geo. of Uinta Mountains, Meso.~()i)' and Crruozoic Oeofo(/i/ hhiI Pd/d'onfoloifi/. 12.' Dr. V. V. Ilnydcii* s!vi3.i feet, and another section on Gunnison river, opposite lioubidean's cre(;k. measured ()87 feet. The estimated tiru-kness, howevei', incliuling the Fort Pierre Gr(»up, is from l,r)00 to 2,000 feet. On Coal creek there is a blulf, in tlie face of which are exposed l,r)00 feet of light-gray and yellowish sandstones and shales, referred to the Fox Hills Group. And on the North Fork of the Gunnison the exposures are of greater thickness. On the ridge dividing Oh be Joyful creek from Anthracite creek, near station :]2, a section of sand- stones occurs 883 feet in thickness. .Most of these sandstones have a metamorphosed appearance, and the ridge, in which they are ex- posed, is intersected with dikes. Below the strata of this section there are pro[)ablv 1,000 feet of siiales and sandstones to a series of coal-bearing strata on Oh be Joyful creek. The latter, according to Mr. Holmes' estimates, is about 2,000 feet above the Dakota Group. Above these beds there is a series referred to the Lignitic Group from 7,000 to 8,000 feet in thickness, covering a large area extending from the Grand river to the Gunnison, beneath the basaltic i)lateauf'i west of Roaring Fork. The strata are conformable to the underhing "^'Tth Rep. U. S. Ueo. Sur. Terr. :,i^ ▼T* 120 CrefnceoHif. ' \ Fox IHIIm rin)ii|), mid it is «litllciilt to (Ictcrmiiic! wlicro oiio foiinntioii ("IkIm iiiid the next Ix'yiiis. From Dr. I'c.'ilc's t'Xjiniination niid study he (!uriii<;' heds casi of the rnoiiiitfiiiis in ('olortuhx arc tlie ('(imviilciit of tlio Fort Union (Jron|> of tlic IJpixT Missouri, and ill*' Koci'iic'rcitiary ; ;dsn that llic lower [mil of the jiToni), lit loiist at the loenlily 'JOO miles east of tlu^ mountains, is tlie equivalent of a part of tin; liujnitic strata of Wyoming'. '2. The Judith rivei- Ixnls have their equivahMit alon^' the eastern edge of the mountains l)el.)\v the Lignitie (»r Foil I'nion Group, and also in Wyoming, and an^ ('retaeeoiis, although of a higher horizon than the eoaldjearing strata of Coalville and Heai- river, I'taJi. They form either th(^ ui)[)er i)art of the Fox HiIIh Grou[), or a group to be called No. 0. ;{. That the upper part of the Fox Hills Gioup is wanting in man3' p.'vrts of Fast(M"n ('olorado, and when presi.'ut seems to he thin and destitute of eoal. F. M. Endlich surveyed the San Juan mining distiiet, where he found the Dakota (Jrotii) resting: uneonformahly upon carbonilerous sandstone. It eonsists of sandstones with occasional remains of plants, and has an estimated thickness of SOO to 1,000 feet. The Fort Benton Group, consisting of dark-gra}* shales, subject to considerable erosion from the action of watei', is found from 400 to GOO feet in thickness. It contains beds of coal. These groups are also developed on the San IMignel anil on the Rio Dolores. A creek flowing scarcely five miles has at the junction with the San Miguel a canon 1,005 feet in depth. The entire canon is cut out of the strata of the Dakota Group, and yet the whole thickness is not exposed. Prof. Loo Lesquereux found the flora of Point of Rocks related to that of Black Butte by nine identical forms or one-third of its known species, notwithstanding that • lere are two to three thousand feet of interposed measures. The distance between the two localities is only eleven miles, and the superposition of the strata is exposed so that the vertical thickness of the intervening rocks may be easily ascertained. He explained the scarcity of the bones of animals in the lower beds of the Lignitic, b}' the fact that, no animal, not even man, if once im- bedded in soft [)eat, can get out of it, and also bj' the further fact that the coriaceous, ligneous plants of the bogs are not food for mammals. He described, from the Lignitic at Point of Rocks, F'ucus Ugnituni, Mesozoic oiut Coiinzoic Geolofjij untl J'uhi niiftdi)i/ij. li»7 Sfilriiu'd nlleiinntii^ Sn/iiifine/id J'lih'dfn, 8. hnuainfn, Si'qnnln hl/onnin, lyiili/riiit/foiiin c(/n)j»hnmfii, I'isfin rttn'iiifufn, Otlelin iiuui'icomi^ J)i'i/o/tLi//finii. I't'iiiiifinii, I), sii/t/'iili-tif II in . il h up II I IIS niefiin/t/ii///if, Lmu'iis {tn.icsfitus, I'thnnimn fofntiih'joh'uiii, (ii'aviojMi.s rji'hitnii, llliiis iiieinhi'iiiniri n ; iVoiii Alkilli Sliilioii, Aliiitcn iiii:i/ii iifiriills, ,1 iiijhiiiH iii'/,-n Jfnoi'tleit, I'iltnr- iiiim />liii.itii,(ji(len; from Suiilli I'nrk, nciir ("iistcllo riiiicli, //i/pmnn hiii/ilciii; from (JijiimI Ku^^Ic .Fnnclinii, /.jn/oi/iinii iiiiirriiici; iVuin (JoMcii, Ziiiiiii>sti'i)lniH m/ru/niis, Animlo i>hliixti, I'tilimwih'.,^ ifu/itiiiuns, now (jfc.inioinifcs ijolitniins, Sahul coiniiiiiiils; IVdiu Miildlc I'juk, Jli/ricii iiisiuiiin, (JiufMiiiii luteniieilfii; iVoiii l'"(>!l Ftsttcriiiiiii, Ih-fiUn ijoydcsl; iVoiu I'leiisiiut Park, IMiiiii cici-k, l-'ii-ns nnills; :iihI IVctin Kvaiistoii, Ficiis pseiKlii-jfojmhts. He (lescri 1)0(1, IVout tlu' Dukot.! Group, iic'ir Fori Ilurkor, Khiihhs,* 'Seqiini.n cotiillfn, Jfi^n'i'n rt'efucnti, Dri/oji/ii/l/mii Infljoliimi, Ficiis ih'.i- toi'tit^ F. l(iiiroj*/iijl/ii, Liinriis pfiil.cav/i»\iii\, l> miles from its mouth, Fasciolaria yrdcilentd; from the Fort Union Gi'oup, at Clea' F'ork of Powder river, Montana, /li/drohia cii/ihioidcs: from the Judith River Group, at tlie mouth of Judith river, ^Montana, Hi/drobia sHbeoni'cd, and Vulvdta inimfauensis. ••■■ 7th Rep. Ilaydcn's U. S. Geo. Sur. Terr. t Invert, Cret. and Tert. Fop:'., vol. ix., Ilaydcn's Sur. V2H Crefaceoiis. 1 ^ ^ li, P. WliitlicM* (Icsci'ilxMl, from the Judith River Group, at the uiouth of Judith I'iver, '/'apes monfanenHh, Jlacf.ra iiiaia^ Sanyniiio- hiri.ii ()bl(if((, und 'I'/iraciu (irinnellL W. -M. (iabbf desoi'ihed, from tlu; (.'retaceous of New Jerse}', Penta- criims l/rijdin', Croiilaslcr iiKniuni/lafji, Scalpelliiik ronradi, IfuHfilns hryain',^ Snrcida sfj'ij/osa, O/tnlut fhomasi, 0. cijtdosfoma, Laxisjiiro •luiubn'cah's, Oslrea firi/aiif, Pdliurtis fridiKjuUn'is ; from the Tjipley Groii[), of Nortli Garolina, E.rlb'fusiis /rem', Fascio/d/'ia kevri^ F. oh/iqif.f'cos/afjf, Gijrofro/tis .sqif(tiiK>.sn,s, Atdphrns kerri, Idonearcn envoi Inensis : from Patula crr'-ik, Georgia, Drillin sfiiHys t'liihrirdn'ns, C. rto'iolosKs, Poli/f/iorax m/'ss'onn'eiisis', II c.dronrhns sfenificrtfi, Ceratodiis erifci- ferns, V. ht'erof/Iijp/tihs^ Mi/lc[oiit;in:i, Uri>ni(nfiis cetlfarniis. Prof. O. C. Marsh* described, from the ui)pin' Crotacooiis of Western Kansas, Ichtkiiornis vir.for, Jli'.sperornh ijracih's, Lestornis drns.sipes, Pferonodqn compfAis, P. in(jcns, P. fontficeps, P. occidentalfs, P. relax, and P. (jrucUis, now yi/cfos(iiirn.s i/r((ciJis. In 1877, Arnold Hagiief estimated the thickness of the Cretaceous on the outl^'ing ridi^es and foot-hills, east of the Colorado range, as follows: Dakota Group, :?00 feet; Colora(U) Gi-oup, 1,000 feet- Fox- Hills Gi'oup, 1,500 feet; and Laramie Groui), 1,500 feet. The Dakota beds arc essentially a sandstone formation, and as they lire usual!}' hard and compact, frequently almost a quartzite, the}' form a wcU-delined horizon. Lying- between the easily-eroded Jurassic marls and clays below, and the overl^'ing blue shales, clays and crumb- ling rocks of the Colorado Group above, the Dakota beds are usually a consi)icuous feature in the ridges, which form the foot-hills of the mnin range. In api)roaching the mountains from the Great Plains, the Dakota beds are especially prominent, as they form the outlying mem- ber of the series of upturned sedimentary beds, whicih risG so abruptly above the plain; for although the overlying Colorado group is pei'fectly conformable, tiiey never occur high up on the long ridges, which form a sort of barrier between the Ict'cl countr}' and the mountain region be^'ond. The Colorado Group is used to represent the Fort lienton, Niobrara, and Fort Pierre Groui)s. The Fort Benton Group is onl}' exposed along the base of the abrupt ridges, and consists of dark, plastic clays, at times distinctl}' bedded, and fre(inently occurring as thinly-'aminated paper shales. The lower beds are always more or less arenaceous, with int(!rstratifi»!d beds of purer clay, while the upper beds sometimes carry thin seams of argillaceous limestone, which, in man}' places, can not bo distinguished from similar beds in the Niobrara. Along the Laramie '■' Am. .Jour. Si'i. and Arts, 3d Scr., vol. .\i. t Ueo. Sur. 40th parallel. i:ui Crefnceovs. I Hills, this group is somewhat difficult to rocognize, but in Colorado it may bo traced for long distances in well defniod north and south linos. The Niobrara Groui), although much thinner, is more easily recog- nized. It frequently blends so completely with the overlying Fort Pierre Groui) that it is extremely diflicult to sej^arate them. The Fox' Hills Group, east of the Colorado Kange, is characterized throughout by great uniformity in texture and physical habit, and con- sists of a coarse sandstone formation, sliowing only variations in color from ro(Ulish brown to reddish yellow. The strata pass by imperceptible gradations, into the Laramie series, ottering^ no »vcll -de lined line of separation, both formations from top to bottom consisting of coarse sandstone. The Laramie Group may be traced along the Big Thomp- son and Cache la, Poudre valleys, and then eastward up the valleys of the northern tributaries to the South Platte. The sandstones form the exposed banlcs along. Crow and Lone Tree creeks, and may by traced northward, passing under the Tertiary of Ciialk BluHs. This group includes the valuable coal deposits at Erie, and the ^Marshall and Murpli}' mines, north of Golden, extending from within one-half mile of the base of the range far out upon tlie plains into Eastern Colorado. The Laramie beds form the uppermost members of the great series of conformal>le strata that lie upturned against the Archaean mass of the Rocky mountains; all ovei'lying strata resting unconformably upon the older rocks. The Cretaceous locks are distributed over the surface of the Laramie Phiins. On Rock creek, a branch of Medicine Bow rivei-, north of the Little Laramie, and near Rock Creek Station, tiie Fort Benton Group is exposed from ;]50.to 400 feet in thickness. In the Norih Park, the Dakota Group is estimated at 3r)0 feet in thickness, and here the Fort Benton. NioI)rara and Fort Pierre Groups have a combined thickness rougldy estimated at from 1,500 to 2,000 I'eet. The Medicine Bow river, after leaving the mountains, runs almost exchjslvely through beds of Cretaceous age. its course being guided by the clays and marls, and the overlying Fox Hills sandstone. On the northern slopes of Elk Alountain, tiie most northern point of the ^ledicineBow Ranae, are found all the beds from the coal measures to the Fox Hills sandstone, uplifted at Ifigli angles, lying against the Archaean formation. All the geological divisions are well represented. In the valley of the North Platte river the Fox Hills Group has an esti mated thickness of between ;5,000 and 4.000 feet. The strata containing the coal beds, at thetown of Carbon, f)56 miles west of Omaha, Mr. Hague supposed to be Upper Cretaceous. m Mesozoic and deaozuic Geology and Piilmoiftohxjy. i:u S. F. Eimiions,* geologist of tlio division west of North Phitli". suiil that Bridger's Priss, wliicli t'onnocts tlio vnlU'ys of tlio rppi'V Stige cTcek and the sonth fork of the Little ]Mnddy, liiis been eroded out of the soft beds of theColortidoCretiieeous. Along the northern and western borders of this valley extends a ridge of white massive sandstones of the Fox Hills Group, standing at angles of ](>° to ^f)*^, and curving in strike approximately with tlie shape of the ridge. To the north of the gap, they f(»rin aeontinuous ridge about 1") miles in length, showing a bluff face to the southwest toward liridger's Pass, at the base of which are exposed the clayc beds of tlie Colorado Group. A thick- ness of 3,000 to 4,00'^ feet of heavy-bedded sandstones, mostly white and butf, with a few includ(Ml beds of shale, and some thin seams of coal, dipi)ing to the northward at an angle of 10° to 20°, is ex])osed. Tn going northward from a point on the Little Mudd)'. about five miles west of the Sulphur Springs, a thickness v)f between 3,000 and 4,000 feet of beds of the Laramie Group, di[>ping northwest at an angle of 20°, is crossed. Of these, the lower 2,000 feet are composed of massive white and yellow sandstones, in which the shale beds are of subordinate importance. The up[)or sandstones are stained and stripe ^. in red, by iron oxide, ami form ridges with considerable clayey valleys between. In the upper 800 feet are several coal seams, and near the top is a pi'ominent bed of bright vermilion color, only a lew feet in thickness, of line-grained, hard, argillaceous material, abounding in well j)i'eserv(!d impressions of leaves. This is overlaid by a white sandstone, about 200 feet in thickness, carrying a coal seam, which in turn is capped by a thin-bedded brown sandstone, which weathers into flags about three inches in thickness; the dip of these upper beds has shallowed to 10°, and to the north the beds of the Laramie Group ai'e practically- horizontal. The exposures of the Fox Hills Group, as seen in Bear Ridge, near the valley of the Upper Tampa river, show a series of massive, white, fine-grained sandstones of several thousand feet in thickness. The Cretaceous of the Uinta Mountain region consists of over 10,000 feet of beds of sandstones and clays, carrying coal seams,which are most abundant in the upper part of the scries. The Dakota Groui) consists of about 500 feet of rather thinly-bedded sandstones, with some cla}- beds, having at its base the persistent conglomerate carry- ing small pebbles of black chert. The Colorado Group, about 2,000 feet in thickness, is made up mostly of clays and 3'ellow marls,, with I * Geo. Sur. Wth iiarallel. f'! ir^ 1:51' Cretaceous. ^v '% some sandstones jit llie base, whieli inclose one prominent coal-seam; the outcroi)s of this groni) are generally oecnpied b}- valleys. The Fox Hills Group consists of about 3,000 feet of lu-avily-ljedded white sandstones, with a few coal-seinns and ('(»mi)!iriitively little clay. The Laramie Group, whose actual thickriess is not dellnitiily ascertiiined, consists also of gray and white sandstones, often iron-stained, contain- ing a greater develoi)ment of clay beds, and very rich in coid seams. It is ovfcrlaid by an unconformable series of beds. The fauna of this group is brnckish, and, locally, even fresh watei' forms are found asso- ciated with marine types. In the valley of l^itter creek, the Fox Hills Group is estimated at 3,000 feet in thickness, and the Larawiie at G,0()0 feet. The latter is characterized by the greater development of clayc}' beds, and hy the great number of coal seams, and by the j>resence of great quantities of leaves and plant remains, especially in the ui)i)(n- })ortion of the series. The beds are conformable, and were evidently deposited prior to the great period of plication and uplift in which the Rocky Moun- tains and the Uinta and Wahsatch ranges received their main elevation. West of Bear River City, in I'tah, along the face of the hills north of Sulphur creek, are exi)Osed outcrops of the Fox Hills and liarainie Groui)s, from 5,000 to 7,000 feet in thickness, standing at angles of 85*^ to 90° west, and striking north 30° to 45° east, and consisting of heav}' white sandstones with conglomerate beds, and passing to the westward into reddish lirown sandstones. The beds of the Colorado Group west of the sandstone ridge, at the bend of Sid[)hur ci-eek, expose a thickness not less than 5,000 or 0,000 feet. About two miles west of Bear River. City, a railroad-cut, through a low ridge running out from the high ground forming the northeastern wall of the Suli)hur Creek Valley, shows a section of about 150 feet of beds, separated by an interval, bare of outcrops, from the sandstones west of Bear River City, but corresponding with them in strike, and standing with an incli- nation of 70° to 80° to the southeast. It is formed of sandstones, inarls and clays, with a few bituminous and gypsiferous seams, and is remarkable for the fine definition of its bedding-lines, the strata varying from half an inch up to a foot or more in thickness. The strata abound in fossils of fresh and brackish water t^-pes, viz.: f/i/o, Cor- hvla, Ltmnaea, (Janipelomn, V/cipnrifs^ctc. They evidently belong to the conformable beds of the Laramie Group, and are overlaid a short distance to the north by horizontal strata of the Vermilion creek Eocene. 3fesozoic (I lid Canozoic GeoUxjij and Pttlaoiifd/orjij. \',','.\ G. K. Gilbert* Ibuiicl tlic Cretaceous strata well displaced upon the Hanks of the Henry Mountains, in Soutliern Utali, where tliey consist of I'our priiu'ii)al sandstones, with intervening shales, and have a thick- ness of ;),r)0() feet. They also contain thin l)eds of coal, one of which was objjerved at the foot of Mount Kllen, four feet in thickness. The lower 500 feet he rel'erred to the Henry's Foik Group. Dr. A. C. Peale,f geologist of the Grand river division, said that the massive, yellow silicioiis sandstone, in some places quartzite, at tlie base of the Cretaceous, is so well defined lithologically, that there has never been any dillicidtv in separating it from the overlying shales. Along tlie edge of the i)laius in Colorado, it is underlaid bj' greenish shaly beds, sometimes lignitic near the top, generally in part or wholly covered, which have always been referred to the ui)per part of the Jurassic, In the West these shaly beds still persist, and the mtissive sandstone, although still recognizable without dilliculty, is much thinner, being only from 50 to 100 feet, and as we desicend, in the sec- tions carried bcjlow, we find othei' beds of siiicious sandstone separated by shaly beds that are arenaceous, calcareous and argillaceous. In these beds, in 1874, he found a sassafras-leaf, which led him to refer them to the Lower Cretaceous. lie drew an arbitrary line sei)arating the Cretaceous and Jurassic. The beds below have the same lithologi- cal characters to the top of the red beds, with this exception, that limestones occur more frequently toward tiie base. In Arizona, G. K. Gilbei't found Jurassic and Cretaceous fossils, associated in beds, re- send)ling those usually leferred to the Jurassic. He is of the opinion that we can not draw any line between the two formations, paheontolo- gically, or lithologically, but for convenience in description it is best to draw an arbitraiy line, which may be changed as we obtain more facts in relation to the formation. There is a narrow outcrop of the Dakota Group on the south side of the Gunnison, above the Grand Canon, between the breccia and the granite. It appears, and .is faulted, at the head of the Uncompahgre river and on Dallas Fork, the latter stream lowing on the line of the fault. Between this creek and the San Juan Mountains it rises until it reaches the summit of the foot hills, appearing from beneath the shales. On the Uncompahgre plateau, it dips gently to the eastward, and is the surface formation until we approach Escalante creek. Be- tween the latter and Roubideau's ci'eek, there are some isolated •■ Kep. on 'the osed at intervals down to The Fork, and also on Smoky and Pine rivers. On the latter stream the exposed thickness is esti- mated at 1,700 feet, and contains four thin seams of bituminous coal. Prof. George ^I. Dawson, who explored the country between the o2d and 54th parallels, in British Columbia, found the equivalent of the Shasta Group in the vicinit}' of Tatia\'oco lake. Along the eastern shore of the lake these I'ocks overlie those of the porphyrite series. The}' dip eastward, or away from tlie anticlinal axis, in which the Irke lies, and form, at a short distance from its eastern margin, a rampart- like wall of mountains, from 2,000 to 3,000 feet high, and twelve miles in length. The rocks are compact, l)luish-gray quartzites, or hard sand- stones, and conglomerates of all grades in regard to size of particles, associated with blackish or dark colored slaty and shaly beds, which recur frequently at dilfei'ent horizons. The thickness of the entire Cretaceous series on the east side of Tatlayoco lake is estimated at 7,000 feet. Their geographical extension is also great. He regarded the Jackass Mountain Group as the eciuivalent of the Shasta Group of California. •'■' Geo. Sur. of Canatln. 136 Crefdreoim. M m % Prot. E. D. Copo* callod tlic Juditii Rivor ( Jroiip No. 6 Cretiiceous. He showed its conlbnn.'ibility with tlu! underlying inaiine Cretyceous, and gave a section ;]:)2 feet in thickness, though its nijjxinimn is not less than oOO feet. His section in ascending order is as follows: Arenaceous marl (with Dinosaurian bones near the top). . . . 12') ' Sandstone, 1st «'> Sandstone fi Impure lignite 2 Sandstone, 2d 10 Impure lignite 4 U)t/o bed 30 Kusty sandstone (with fresh water shells) 25 Arenaceous marl (with petrified wood) 50 Sandstone, .*kl 15 Marl 20 Reddish shale 10 Lignite 5 .Shale 7 Black shale and lignite 3J Bed of Osfrea subfr/ffonal/'s 15 3 B X teet. (( u ii (I (.' ii, u Ci a a a a Total 332^ feet. The presence of Dinosaurians, gar fishes, turtles, Physn, i-^lnparus and Unio prove the fresh water character of the strata, while the Ostrea indicates a return to brackish water. Dr. C. A. Whitej described, from the Judith River Group at Gov*' Island and Dog creek, a tribu'tary of the Upper Missouri river, in Montana Territory, Unio cryptorhynchus, JJ. senechis'^ U. primaevus, Anodonta propnforis, Bulrnus dJavus, and Physa ropel. Prof. F. 1>. Meek;]; described, from near Laporte, Golorado, Anomia rcRtiformis; from East Ganon oreek, Wasatch Range, Utah, Cucnllma obl/.qiia, Jlactra emnionHi; from Goojjer creek, Laramie Plains, Wyoming, Axmcua Wyoming ens is; from Red creek, Uinta Mountains, Utah, 3Iactra orenoria; from East Ganon creek, U^tah, Mactra utah- ensi's^ Tellina isonema, T. modesta, Gyrodes depressa, and Anchnra fusiformis. Prof. G. A, VVhite§ described, i'rom east of Impracticable Ridge, Utah, Osfrea prudentio; from near Pueblo, Golorado, Inoceramus * BuH U. S. Geo. Siir., Vol. 3., No. 3. f Bull U. S. Geo. Siir., Vol. 3., No. 8. t U. S. Geo. Expl., 40tli parallel. ? Wheeler's Sur. W. 100th Mer., Vol. 4. \ '4^ Mesozoic nn- an aggregate thick- ness of between HOO and 000 feet; tiic lower half consisting of a dark- colored, coarse, silici'dentia, Odontobasis formosa; from Black Buttes Station, Wyoming, Unio goniambonnfus, U. aldrichi, NeriUnn bapfista; from Bear river, near the confluence of Sulphur creek, Wyoming, Acella haldononi, N'eri- * Bull. U. S. Geo Sur., Vol. 3, \o. 3. t Am. Jour. Sci. and Arts, .Sd Sor., Vol. 14. I 10th Hop. llayden's U. S. Geo. Sur. Terr. g Bull. U. S. Geo. Sur.. V^ol. 4, No. 3. ^WT^ m Crcfdceoiifi. fina 11(1 ft CI form is, l^ltu'ftnrtin coiicsl; IVom near Evnnston, Helix eva ti s f aliens is ^ and fSoniolxisis eiullichi. Prof. Leo LiisqiK^rciix* (IcscrilxMl, tVoin the Fort Union Group, at Black Htittcs, Wyoniinir, Scqiutia acinninnhi, Vitis sparsa, Orenu'opsis saportdiKi, G. fcnui folia, Jifius psciuhnnevia iil, Podoiionlnm omeri- canum, Carpifes iniji'irdrinnj'. (jl atiuffonnis^C mifrttl Ha,C . verrnrosiis, C, ribiirui, C. bio'str/onnis; IVoni Oohh'n Soiitli Mountain, Colorado, SiahnJifcs fr'iirfifer, Pdhiiocdt'pon (runcatiun, J*, com' f/ a turn, P. snbcy- linth'icinn, Popiihis iintjeri, lAiiirns oroteoidcs. VibtirniDii auceps, V. (loldianinn,V. solitper tliird the shales are more arenaceous than lower down. A cold sulphur spring near Camp IJrown seems to take its rise in these shales which must be regarded as a vvvy proliiic source for alkaline com- pounds of a highly soluble nature. 'Witliin the shales tiiere are snuiU inclusions of i)yritc. I'pon dccomixisition of this and tlie shales various salts are formed. The thickness of this group is about GOO feet, increasing southerly to J)00 fecft. ;j. The Fox Hills Group, consisting in the lower [)art of brown and yellow shales, interstratided with thin beds of sandstone. Some of the shales are very dark and carl)onaceous. Above this alternating series there is a considerable thickness of yellow and brown shales. As a rule, they are arenacernis, but some of them (piite IVee from sand. Small particles of mica occur throughout. Higher up, sandstones set in again, containing, together with thin seams of shales, small deposits of coal. The upper i)art is formed b}' thinly-bedded, micaceous and argillaceous sandstones, covered by a thick stratum of the same material. The thickness is estimated at 500 feet. About two miles west of Cam[) Brown, a xcvy interesting hot spring occurs, wi^ich rises in the beds of this group. It is kiiow-n as the Hot Sulphur Spring. The temi)erature is from about 100° to llO*^, and varies but little with the weather. The bright green and blue water is contained within an elliptic basin 1)15 feet long and 250 feet wide. A constant bubbling up of carbonic-acid gas gives it the appearance of boiling. The mineral constituents held in solution by the water are iron, lime, magnesia, soda and potash. They seem to be conttiined in the form of sulphates, carbonates and chlorides. The heat which sup- plies the warmth of the water is supposed to be due to chemical changes going on within the strata through which the moisture finds its way. A petroleum spring also occurs near Camp Brown, originating probably in tlie same rocks. The Laramie Group consists of a succession of shales and yellow 140 CrcfnceoiiH. hiindstont's, forming low, lono-coiitiuiu'il lilnlls. Tlif lliifkiu's.s is csti- iiiatnl iit 400 foot. The yellow jind whiti' sjiudstoiics of the Dnkotii nroiip oocur in the northern portion of tlic Swcotwutcr nills. Kasl of Kililiorn (Jap tlu'v arc much folih-cl ami jilicatcd. In U'iiis! siiinlHtiUM's, coiitMiiiiiijj: beds of ('(»!il. .mihI iIiiiU ;iii(l of'tc'ii (•!iil>()ii;it'('(>ns Hlinl«'^. SamlstdiicH intMliiitc tin; triiiisitioii iiilo the lower 'rciti.'irv Lfrotips. Tlu' lower coiil-hori/.oii is the most prcMlm-tivo. The tot.'il tliickiicss of this yroiip west ol" Wtiwliiiu-^ Spiiiins, and from then' northward, is estimated at IjKMi feet. The decomposition of pyrite in dumps from coal liaiiUs. pr(»diiees a spontaneous coml>iiHli(»ii of the coal which chiUi^'cs the I'olor oft lie shales to a lirilliaiit vvA. In the same maiiiier prohaldy tliei'itisli Columbia, on the headw.ateis of the Skayit, wi^st ot the main axis of the ranjie. which forms the watershed, between that river and the Similkameen. The trail traverses the area in a j.reneral northeast direction foi- nearly thirteen miles. A section occurs on the trail immediately east of the crossing of the north branch of the Skai^it, repi-esenting a thickness of 4,420 feet; The rocks are much disturbed, are lying at all angles up to vertical, and have suffered considerable hardening and alteration. They consist, generally, of sandstones, conglomerates and argillites. Still further north-westward, from the vicinity of the mouth of Ander- son river and Tioston Bar, they were found to extend, in a long, narrow trough, nearl}' coinciding, in the main, with the Frazer river, with a general bearing of about N. 70° W., to the vicinity of Lillooet and Fountain, a distance of about 80 miles. The estimated thickness is ■:• lltli Ann. Itep. l'. S. Geo. Sur. Torr. V (iuo. Sur. of Clin. r ■» "•^ 142 Crefaceons. 5,000 foot, Tlioy were also roiiiul on tiio Tlioiiipson, l)el(»\v its junction Avitli tlio BoiuiiKirLe. Tiie thickness on Tathiyocc*, 220 miles north- eastward from Sivagit vaUey is estimated at 7,000 feet. These rocks are regarded as of the same age as the Slmsta Gron[) of California. Prof. C. A, White* described, from tlie Fox Hills and Fort Pierre Group, at Cimarron, New Mexico, Caryophnllia johaiinis^ C. eyeria, Cra.s.safclid cimnrronensh; from Ililliard Station, U. P. K. R., Wyo- ming. Placimopsis /tilliardensi.s, Nerltitui iticonipta; from Coalville, Utah, NerUinn pafelliformis, var. veberensis; from INIonument creek, near Colorado Springs, Palinrns 2}e)it((nyt(lntiis; from the mouth of the Saint Vrains, Northei-n Colorado, Barodo suhelUpticc , Parhymya kersey i, Actneon irnosteri, A ctaeonin(( 2>roso(iheila ;^vo\Vi west of Greeley, Colorado, T'ltK-i'adid coelionofAfs, Ghjclmeris berthondi and Anchi'ra ha !/ d e )i >'; fvom the Cretaceous, at Salado, Bell County, Texas, Exoth of this irreat area, and far tlie greater part of the other extensive and nu.merous displacements which the strata of the ditferent i>eolo be swjtUowed up by another name for tlu; same group of rocks. A great many synonyms have been i)roposed for this Group, some of which it is ditlicult to wipe; out, and others will l)ui'then the science for a longer or shoi'ter period, but, finally, we may hoi)e for their burial in oblivion. Any one can propose to call an exposure of rocks, at any i)lnce, by a new name, but it requires a paheontologist to determine the age of the rocks and to refer them to their pioper posi- tion in the geological column. A little reflection, therefore, will satisfy the reader, that proposing a new name for a grouj) of rocks, wherever exposed, without giving the palreontological reasons for so doing, is an evidence of ignoi-ance, and most frequently we find those who do it are suffering from downright stupidity. The plants which have been described, from the Cretaceous rocks in (piestion, have l)een referred to about 150 genera, and number about HOO species. About 50 of these genera are now extinct, and about 100 are living. The larger part are from the Fort Union Group of the West, and from tlieir intimate relation with living forms, the great pala?o-botanist. Prof. LeSquereux. referred the rocks to FiOcene age. Tiie testimony, however, of the animal remains, which Prof. Cope was the first to dis- cover, has proven that they must i)e referred to the upper or later Cretaceous. This determination has, if we may trust investigations of our fossil botanists, specifically united the Cretaceous era with the present time. For the living plants, Oori/liis americana, (J. rostrata, DavdUin fenuifoUn^ and Onorlea sensihlllti have been identified among the fossils from the Fort Union Group. It is likely that too much confidence in this identification may lead to erroi-, for as yet we maj' fairly suppose that we know but little of the vegetable life of this vast period of time in comparison with what will be known in a few de- cades. And better specimens than those upon which the identifica- tions have been made may show s[)ecific distinctions. It is sufficient that the forms so much resemble the living as to be mistaken for them, to show how closely the living forms are connected with the ancient dead. mt 146 Cret.ucenvs. Tho relation between *;lie invertebrate liingdom of the Cretaceous period and the living invertebrates is shown (according" to present identifications) by the survival of more than one third of the Creta- ceous genera, though all Cretaceous species have become extinct. The survival, however, in dilferent classes, is by no means uniform. In tlie class Polypi, of sixteen Cretaceous genera, six are living. In the class Echinodermata, of tweniytwo genera, eight arc living. In the class Bryozoa, of thirty-two genera, nine are living. In the class Brachiopoda, of six genera, live are living. In the class Gasteropoda, of one hundred and seventy-lour genera, ninety-six are living. In tiie class Lamellibranchiata, of one hundred and sixty-four genera, seventy are living. But in the class Cephalopoda, where there were more than thirty genera and subgenera, all iiave become extinct except a single genus, the NnHtilus. The connection between the vertebrates of the Cretaceous period, and the living vertebrates, is, seemingly, much farther removed. No Cretaceous genera of birds or mammals survive. In the class Reptilia, where more than seventy-five Cretaceous genera have been determined, only three genera are known to have survived, Crocodiliis^ IWionyoc and Emys. A few species of fishes, found in the Cretaceous, have been referr- ed to living genera, u.:d probably some of them are correctly so referred ; but from the great differentiation observed in the vertebrates, during tho long period of time which has transpired, we can not ex]iect to find many forms preserving unchanged their ancient outlines, though we may be able to trace backward the living genera into what we call distinct ancestral genera or families. This closes our remarks upon the iMesozoic period, and we will now take up the Caiuozoic. There is no great break in nnimal or vegetable life in passing from the IMesozoic to the Csenozoic, as earlv geologists, fi'om very limited observations, supposed. Indeed, it may be said to be a most propable hypothesis that there are no breaks in genealog- ical trees. All organic life has descended from ancestral forms, and among the vertebrates, in the later geological periods, profitable accre- tions or accessions of important parts or functioi;s have been developed in successive generations. This will become more apparent as we pass from one group of rocks to another in the Tertiary period. Mesozoic and C(vnozoi'c OeoloQi) and Pfdivontoloyy, 147 THE C^ENOZOia AGE. OR TEIiTIARY PERIOD. When the words Primary, Secondary and Tertiary are used to dis- tinguish geologieal subdivisions, the rooks are so coniprelunidod as to leave none to wiiicli the word Quaternary can he pi'operly applied. The organic renuiins of the Tertiary arc; likewise so completely blended with the living organisms, that we can not distinguish a Quaternary age or i)erioil. The subdivision of t.»e Tertiary, with reference to the survival of concholo;>ical species, into Eooene, Miocene, Pliocene and Post-pliocene, brings us to the living species as gradually as the spe- cies are found to change within any of the subdivisions of geological time, or within any of the minor subdivisions of the strata into groups. It is, therefore, evidently a mistake to use the word Quaternary, in a geological subdivision, with reference either to the rocks or their oiganic contents. The Tertiary rocks, generally, consist of marls, clays, sands, or other friable material, filling depressions in the underlying rocks, and, tiu)ugli widely distributeil, seUloin form hard continuous strata. This condi- tion cf the rocks in Europe made it ve:y ditlicult to determine the order of superposition, and led Deshayes to suggest, after having ex- amined 1,122 species of fossil shells from the Paris basin, and having identified only thirty-eight with the living, that a subdivision of the Tertiary might be based upon the relative proportion of the extinct and living species of shells. lie drew up, in tabular form, lists of all the living shells known to him as occurring in Tertiary' rocks, and sub- mitted the same to ]Mr. Lyell. The number of jecies of fossil shells examined by Deshayes was about three thousand, and the living sjjc- cies with which they were compared about five thousand. With this assistance, and that furnished by the works of Basterot and some Italian authors, .Mr. Lyell, in ISIJ:), estimated that, in the lower Ter- tiary' strata of London and Paris, cJ.t per cent, of the species are iden- tical with the living; that, in the middle Tertiary of the Loire and Gironde, about 17 per cent, are living; that in the upper Tertiary, or Subappenine beds, from oo to 50 [jcrcent. ; and that, in strata still more recent, in Sicily, from 90 to 95 i)er cent. He proposed to call the lower Tertiary " Eocene," which signifies the dawn ot the present state of things; the middle Tertiary '• Miocene," which implies less recent; and the upper Tertiary *' Pliocene,'' which means more recent. The ' m 148 Tertiary. U Pliocene he subdivided into the Older Pliocene and Newer Pliocene. In the latter, out of 220 fossil si»ecies of shells, he found 216 to be living. He afterward proposed the name Post-pliocene for rocks hav- ing all the imbedded fossil shells identical with living* species, though they may contain extinct mannnalian remains. We now include in this group strata which belong to more modern time, and which arc fre- quently called " Recent." This subdivision of tho Tertiary, with reference to the survival of conchological species, and the si bdivision of the strata, or rocks, into groups, have made a double system of nomenclature, which does nM prevail in the older geological periods. The determination of the North American equivalents of the European strata, by the per cent, of living species, was soon ascertained to be impracticable, and, instead of that method, the age is determined by the extinct species. Certain species have come to be regarded as types of pjocene age, or Miocene, as the case may be, and, from the presence of these, the rocks are referred to the proper subdivision of the Tertiary. I have not found time to separate the consideration of the Tertiary, into the groups into which it has been subdivided, and preserve the chronological order, or history of our knowledge of it. For this reason^ I will follow the order of discovery in matters relating to the Tertiary, separating only that part relating to the fresh water drift of the central part of the continent, which will form the conclusion of this essa^'; nor will I dwell upon the few vertebrate fossils mentioned prior to 1820. In 1824, Prof. Silliman* noticed the Tertiary exposed at Martha's Vineyard and the Elizabeth Islands. Prof. 01mstead,f in the first re- port ever made, as it is said, in any country, upon geology, with State or Government funds, described the country through which the Beau- port canal was excavated, and separated the strata into: 1st. A black mould; 2d. Potters' clav, of a yellowish brown color; ;5d. A thin layer of sand, full of sea shells and the remains of land animals, particularly v>f the mammoth, from three to eight feet deep; and, 4th. A soft blue clay. Thomas Sa}'^ described, from strata now referred to the Miocene of Maryland, Tarritella jifebeia, Natica interna, BaGchmm porcinum, now Ptychosalpinx x>orcina, B. aratum, Fksus cinereus, now Urosal- pinx cinereas, F. A-costatus, now Ecphora quadricostata, (Jalyptraea * Am. Jour. Sci. and Arts, vol. vii. t Rep. on the Geo. of North Carolina. t Jour. Acad. Nat. Sci. vol. iv., pt. 1. Mesozoic and (Uvnozoir Geohxjii and Palreonloloijy. 140 grandis, now Dispotwa (jrandis, Fi'ssureUa redimicuht, Osfrea com- pressirosfra, Pecteii je^'eraonius, P. madhoniiis, P. clinlonim, P. sep- fenariiis, Plicafnla marginata ; iiiid from strata now refVrrod to the IMloceiie of .^lurylaiul, Avra arata, A. ceiifetKO-fa, A. incile, Pecf.un- ckIiis sifbovafiis, Niicuhi concenfrica^ N. laei'i.s, Venericai'din yravu- lata, now Cardita yranulata, Cnnisdlelln nudiilafa, [socardid/ra/erna, Tellinn aequisti iata^ Liici'no anodonta, L. cordraofa, L. crihraria^ L. suhobliqiia, VemiN de/onnis^ Asfarte undulafn, A. v/'cina, Aviphi- desma sabovatinti, Corbidn cnneata, C. inaeqiKUis, Panopcea rejlexa^ Serpida (puinifern, and Dentaliinn atfenuafnm. In 1825, Dr. Kichard Harlan* described, from Bigbone Lick, Ken- tucky, Ccrt'UH americatiiis, iJus bombifrons, now Ovibos bombifron.s, B. latijrons, now Bison lafi/rons ; from a cave in Oreenbriar county, Virginia, Jlec/alonj/x jeffer.soai^ and from Skidaway Island, Georgia, Meciatheruim cucierl. In 182S, D)'. J, E. Dekayf described, from the Post-pliocene at New Madrid, on the JMississippi river, Jios pallasi. In 1820, Dr. Morton;]; arranged, from the notes of Lardner Vanuxem, sofne geological observations on the Tertiary and Alluvial formations of the Atlantic coast of the United States, showing their great extent and inclination from Nantucket and Martha's Vineyard, f ■ the coast of New pjugland, to the Mississippi river. The moder.i alluvial was divided into vegetable mould and river alluvium; the ancient alluvial into white siliceous sand and red earth; the Tertiary formation into beds of limestone, buhrstone, sand and clay. He described, from strata now regarded as Pliocene. Crcpt'dula costata. In 1830, Mr. Timothy A. Conrad§ showed that Tertiary deposits occupy all that part of ^Maryland south of an irregular line, running from the vicinity of Baltimore to Washington City, between the Potomac river and Chesapeake bay, though most of the surface is covered with a diluvial deposit o( sand and gravel; and from the pres- ence of Tiirritella mortoni, Ciicnlkvo fjiyantea, and Venericardia planicosta, he regarded the deposits in the vicinity of Fort Washing- ton as contemporaneous with the London cla}' of England, which now constitutes part of the Eocene of Europe, This was the first announce- ment of the existence of strata, of this age, in America. * Fauna Americana. T Am. Lye. Nat. Hist., N. Y., vol. ii. I Jour. Acad. Nat. Sci., vol. vi., pt. 1. 'i Jour. Acad. Nat. Sci., vol, vi., pt. 2. ■; 150 Tertiary. *) He (lescribeil, from Afaryland, in strata, now re<;ar(le(l as of Pliocene age, Murex acuticostn, Volnfa soft far/a. Cassis cwlafa/rrochns humilis, T. rcclusas, Pi/rvfa sulcosa, Turritelld laqucafa^ 1\ rariabilis, Can- cellaria lunaf.a; and from strata now I'eferred to tlie Miocene, Xatica frogilis, Pfenrofomu communis, P. (Ussimilis, P. pavva^ P. rotifera, Maryinella denticuhita, N'assa qaadrafa, Terebra simplej; Actaeon melanoides, A. ovoides, Mncfra ponderosa, Venus a/reafa, Amphi- desma carinohim, Area ma.ciUata, and Cardium laqueaftnn: and from strata now referred to the Eocene, Monodonta glandnlo, Turritella morfoiii, CucuUma (ji(/antea, now Latiarca giganfea, t'rassalella alae- formis, and Vcnericardia blandiiu/i. In 18;>2, Prof. Edward Hitclicock* described tlie alluvimn as tliat fine, loamy deposit, whicli is yearly forming* from the sediment of run- ning waters, chiefly by the inundations of rivers. I<; is made up oi the finest and richest portions of every soil over wiiich the waters have passed. No extensive alluvial tracts occur in Massachusetts; although liuiited patches of this stratum exist, not infrequently, along the banks of every stream. The diluvinm.^ he said, occupied more of the surface of the State than any other stratum. It is not generally distinguished from alluvium; but it is usually much coarser, being made up, com- monly, of large pebbles, or rounded stones, mixed with sand and frag- ments of ever}^ size, which are often piled up in rounded hills to a con" siderable height, and under such circumstances as preclude the proba- bility that it could have resulted from existing streams. The Tertiary formation is represented as most perfectly developed on Martha's Vineyard, though found on the Connecticut river aud in the vicinity of Boston, and in limited patches in other parts of the State. He said the difference between this formation and the diluvium is, that in the diluvium, the sand, pebbles and clay are confusedly mixed together; but in the Tertiary, these materials are arranged in regular, and gen- erally, in horizontal layers, one above another. Hence., when the sandy stratum happens to lie uppermost, the soil will be too sandy; but ii this be worn away, so that the cla}' lies at the surface, the soil will be too argillaceous; or if the gravel stratum be exposed, the soil can not be distinguished from diluvium. In 18;5;J,f he treated of the coast alluvium, which is produced by tides aud currents in the ocean, tliat frequently transport large quantities of soil from one place to another, and cause it to accumulate in those * Rep. on the Geo. of Muss., 1832. + Hop. on the Uco. of Mass., Ks33. Mesozoic and (Jctiiozoic Geolotji/ nml I'tdtconf.olofjif. 151 situations wIicit tiio t'orco abates nv is destrnyod. 'I'lio Salt Marsli alliiviiiin, wiiic'li results tVoiii tin; decay of salt niarsli plants; the .silt brouj^hc over the marsh by the tides; and from the alluvial soil brought down by streams which empty through these marshes. Ho mentioned the submarine forests on the coast, and ou Martha's Vino- yard, and numerous deposits of peat, and tlie processes by which it is produced. He observed how ra[)idly the New Ked Sandstone disinte- grates and unites with the soil, giving a decidedly red hue to extensive tracts of land; and likewise the gnoiss. which is found disintegrat(Ml to a depth of from six; to ten feet, and thus covers the earth and ob- scures the rocks even in the hilly districts. Some varieties of trap, sienito, mica, talcose and argillaceous slates are similarly affected, and even quartz ro(^k is shown to slowly decompose by the action of the weather. As evidencing the latter fact, it is mentioned that the name of John Gilpin had been painted upon a smooth boulder of granular quartz within the past 1 ")() years, and that the paint had so protected the surface beneath it, while the decomposing process went on over other parts of the rock, that the name is now found perceptibly ele- vated on rubbing th(» lingers over the stone. Three causes — rains, frost and gravit}' — are said to be constantly operating to degrade the hills and the mountains. In preci[)itous trap-ridges, water penetrates fissures, freezes, and breaks asunder the masses which constitute the slopes of broken fragments or debris of rocks, which arrest the atten- tion on the mural faces of the greenstone ridges in the Connecticut vallo}'. The gneiss rock, in Worcester count}-, abounds with sulphuret of iron, which is continually undergoing decomposition by the action of heat, air and moisture, and becoming changed into an oxide and sulphate. The oxide imbibes carbonic acid from the atmosphere, and is changed into a carbonate which is soluble in water; or this oxide is washed into cavities, where it meets with water containing carbonic acid, by which it is dissolved. Once dissolved, it is transported to ponds and swamps, where it is de[)osited by evaporation, and forms the well known bog iron ore. Rocks containing manganese are like- wise undergoing decomposition, and producing, in a similar manner, the oxide of manganese. The ridge of bowlders on the margin of some ponds, where the bot- tom is free from them to a considerable extent, is accounted for by the expansion of the ice in lifting them from the bottom and vowding them out, while there is no force on the melting of the ice r,o draw them back. ^PIH ir)2 Tcrtidfji. The (MUToacIimonts of tlu? son ii[)i|)per terrace which forms the great valU\y of the Connecticut. The t(Mraces found in the river val- leys are described, and their oric/ci. If. seuieu, now Ifuculana semen, Avioula claibornensis, Pecten destiayesi. P. fyelti. Plicatuta mantelli, Ostrea alabamensis, O, dirarira/a, 0. linyu((canis, 0. pincerna, O. semitunafa, Fissurella claibornensis, Ifippo'iy.'^ pyymiva, now Concholepas j^yymiva, InJ'undibulum trochiforme, (Jrcindula cornuariefes. Bulla sthillairl, B. dekayi, now (Jylichna dekayi, Pasithea aciculata. P. claibornensis. P. eleyans, P. yuttula, P. luyubris, P. minima, P. notata, P. secate, P. umttiUcata, P. striata, now Acto'onella striata, P. sulcatit, now A 151 Te.i'lionj. 4 i*| suli'dfii, IVaficii ./I'hhnsfi, now yeven'fd f/ihhosa, Niitica ma(/noiim- hilicHfd, iV. mamma, JV. nn'iiima, now Linxithi iin'n/'md, y. viitior, N". parrn, JV. seiiu'/utiafa, N. itfriatit, Acffteati e/ecafits. A. Ifievin, .(, h'/iejifiis, .t . miti/noph'ffi/iin. A. pinirfiifus, A. iref/icn'/lf, A. viv.laiivlhis. now OhvJisciis melinic/his, A, >ifrid.fi/ilic(if(i, (J. pnrva, C plied ta, ('. aciilpliiiui, (J. f.essc/lafa, Fascio- Idvid rlei'dfft, F plicAifd. now f.nfittr/is plt'cafifs, Fksks dcdfus, F. bicai'inahis, F. coitjibeio'cf, now Strepsidara coni/benrei. F. crebf.ssi- mus, F.der.nssdfiiH. I\ delabeclxi. F. ^/fffoiii, F. mdfinocostafus, F. minor. F. morfoiiL F. nanus, F. ornafns. A. /).i.'riin, F. pn/cher, F. puiniUs, F. taiti, Pi/rnla canceJ/dfa, P. eleipinfisshna, P. si>nel/its, Luniiin ilolahrn, L. ixindnln, N'ucnhi hclhi, JV. caehtfn, .)fe/otif/(iini oli'Cdhi, now Cnssidti/ns (tl rat fits, (^i'ej)idiilit h'l'tifn, Sohtr- iinn chihordfnm, wow At'chitcrJ.oniiui cbihoratd, Sif/a re/us /ia; at Shell lihill', on the Savannah river, liftoen miles below Anynsta; at Fort Gaines, on the ('hattahoo- clicp, and other plaees; t'loni all which lie projected the continnity of the strata, coniinencing in Maryland, at Fort Wasiiiniiton, and extend- ing in a soiitlierly direction across Virginia, North and Sonth (.'arolina, and westerly across (leoi'gia, Alal)ania and Mississippi. His diagram, representing the strata composing the blntl at Clail)orne, showed, in descending order: 1. Diluvinin, 20 I'eet; !. Whitish, friable limestone, 45 feet, containing Scuf.eUa hjelli ; W. Six feet indurated limestone, wliere the fossils occur in casts; 4. Ferrngiiions, siliceous sand, 14 feet, containing Citrditn jdanirosfa, Corhfs Iditiel/osa, and PynuDi'delht tereheUfifa ; 5. Sand, with a calcareous cement, 3 feet, containing 0.s'- trea sellaeformis ; 0. Soft, lead-colored limestone, 70 feet, containing O. sellaeformis in al)undance, and rarely PhKjiosfoma dnmosum; 7. Frialile, lead-colored limestone, of unknown thickness, containing Cnr- dita planicosta, a shell very characteristic of the Eocene. He remarked that the Plagiostomn dtimosuin [)assed from the cretaceous rocks to the Eocene; that the Eocene at Claiborne appeared to be older than the Eocene of Europe, and older than the deposit at Fort Washing, ton, Md, He described, from the p]ocene of the Southern States, Tellina scnn- dida, Pectunculus pcrplanus, now Litnopsis perplana, Fusus irrusus, F. raphanoides, F. salebrosns, F. sexayigtdatns, F. symmetricus, Cassis breviaostaf/us, C. taiti, Cerithhini nassula, C. solitariain, Ancillaria * Am. Jour. Sci. and Arts., vol. xxiii. i Jour. Acad. Nat. Sci., vol. vii,, part 1. I": 'I 156 Tertinry. I' tenera, Fhsus coopcri, now Clavifiisas cooperi, Crepidiiln dnraosa, Mnrex mantelli, 3F. sepf.emnarins, IVrehrn poliji/ijra, Serpula sqiiamu- losa, Cjjfhered nuf.f(tllt', C. inortonl, Ostrea (jeorgiana, and Sciitella lyelh\ now Mortonia hjellt; und from more recent Tertiary r*f the Sonthern States, AnatuKi. antlqiia, now Periploma antiqua, Saxi.cavn pecf.orofia, Pa lorn areno'^a^ Tellina dec/iiu's, T. ef/eiia, Cytherea •ho- vafa, C. pffnddid, C. reposta, Aviphidesmn suhrejlextnn, Asljirte '..on centrica, A. Innulafa, A. obni/a^ A. symmetrica, Balanus pyofeiis; Fascinlaria muiabilis, Tii7'biiie//.a donissa, Canrellarla. perxpectiX't, ('.. plttfjiostomn, Trochns be/fas.^ T. labrosas, T. InpidosKs, T. ^nitchelH, T. phihintropus^ PleHrofoma hiscafe/iaria, P. fiicil/fera, P. j>yreiioidcs, P. fricatenari't, P. viryiniaaa. Turbo caperaf.ns, Manjinella ebnrneola, 31. Ihnafiila, Solarium anperum. now Archifectonica nupera, Delphi nuhi lyra, now Carinorhis lyra, Actoion novel/ us, Deiif.a/ium fhallns, Fissurella alticostn, F. (jriscomi, fn/nndibuliim r/yrini'/m, Capnlus higubris, Turrite/la alticosfata, T. oatonaria, Cancellaria alfernata, Pecten decemnarins, P. royersi, Lepton mactroides, and Tellinn bipli- cata. He also nicntioned the following Pliocene fossils, wiiich are to be found living on the coast of the United States, to wit: Area transversa, Cytherea sayana, C. yiyantea, Pholas costata, Ostrea virqiniana, Soleii ensis, Amp)hid?,sma inequale, Saxicava rugosa, V^ni's mercenaria. Panop)ea rejlexa, Jfactra tellinoides, Pandora friUneala, Cardita fri- denfata, Lucina conlraeta, L, crenulata, L. divaricjita, Corbida con- tracta, Crepidulata convexa, C. glanca, C. plana, Lafraria canalicu- lata, Fnsus cinerens, Wassa trivitfata, N". liinata, Nafica duplicata, J^. heros, Fulgnr carica, F. canaliculahis, Jfactra lateralis, Scalarin clathrus, and Vermetus lumbricalis. This list does not include fossils of the newer Pliocene. In 1836, Trof. Ed\:ard Hitchcock* described, from the Miocene at Portland, Maine, Nucala portlandica. Dr. Samuel G. Mortonf described, from u Miocene ' r Pliocene de posit, near iMarietta, Ohio, Unio pctrosii.s, U. saxulum, U. terrenus, U. tumiflati/s, and Anodonta ahyssina In 1837, Win. li. and Henry D. Kogers;]; described the Tertiary- in the counties of Elizabeth City, Warwick, Yorii, James City, Va., and the lower extremities of New Kent and Charles City, having a total lengtli *Bost. Jour.Nnt. Hist., vol. i., pt. 3. t Am. .Ii)ur. Sci. and Xtis, vol. xxix, X Trims. Am. Phil. Soc, vol. v. Mesozoic a»d C'oiozoic Geology and Pahnonfology. W, t'ligtli of about fifty miles, and a mean breadth of fourteen miles. The super- ficial stratum is au arjillaceo'.is beds of clay are found, of a yellow, blue, green, red or variegated color. In soino places this clay is from twelve to fifteen i'eet in thickness. Below this stratum there is usually found a red ferruginous layer, from an inch ^o a foot in thickness. Beneath this layer there is a yellowish brown sand, frequently containing a large proportion of clay, a!: of which is barren of shells. Below these su- perficial layers occur the various shell beds of Miocene sand and clay, from which these authors described THmteUrt quad) intriafn, T. ter- sfrinfn, N'atica pevsperJiva. Fissirrel/ti cnfilliformis^ Area protrncta^ Liicina speciosa, and Venus corfindi'Ui. They also described, from the Eocene greensnnd, KHCuln raltellij'ormis^ now Nnciilana cnUeUiforniis, K. pan^a, and Cytherea ooata, now D/one ovnf.a. In ISilS, Mr. Conrad* said that the most northern locality known to be decidedly of Medial Tertiary age, is in Cumberland county, N. J., from whence the deposits extend southward in a very connected series, and are spread over a large portion of the Atlantic seaboard. The eastern shore of Maryland is chietiy composed of this and the superior formations, bvit the greensand occasionally appears. The Medial Ter- tiary occupies all tha': portion of the western peninsula south of a line running from Annapolis to Fort Washington, on the Potomac, and nearly all that part of Virginia which lies east of a line ruiu\ing through Fredericksburg, Richmond and Petersburg, to Halifax, in North Carolina, in which State the formation expands to its greatest breadth. Tlie lowest stratum of the Medial Tertiary is clay; the upper stratum sand; and the intermediate strata are composed of sand and day, either pure or intermixed. The general surface of the country is level, and it was originally covered with a forest of pine trees. The western limit is bounded by a narrow strip of the lower, or Eocene Tertiary, which reposes upon Cretaceous strata. He described, from the 'SUoi^enGj 3fy(i prodncfa, Piindoracrassidens, Phohidomyfi ahriipfa, Pdnopntn american( , Corbnid elef((f(t, Venus fef.riaa, V. ducofelt, now Mercendr/a ducatelf, V. rilcyt, Cytherea metastriata, Sphairella sub- rexa, Saxicava bilinedta, JIacfrn iucrassata, Jf. subcuneafa, Vardium acutilaquefttum, Lucina crenulnta., Venus hitisnlcatn. now Euloxa latisulcata, Astarte arata, A. cuneiformis, A. perplana, A. cohenf., P^ *■ Fossils, Tertiary Formations. --T7V 158 Tertiary. PeQten virginkiinis, Ostren percrassa, 0. suhfafcatn, O. srulpfiira(a,0. disparilis^ M ijoconcha iiicxrva, Modiola ditcatelL now Volsella duca- teli, Byssoarca marylandira, and Ai'ca caUip/enrd. Prof. Emmons* (lesfribcd the Tertiaiy of Lake Cham plain as con- sisting of clays and sands, embracing, to some extent, marine shells of recent age — the whole formation in Essex county, New York, not ex- ceeding fifty feet in thickness, and averaging only from twenty to twenty- five feet. From above, downward, the strata are, first, a fine white, or 3'cllowish white, marine sand;, second, a yellowish clay; and third, a blue clay. The yellowish clay abounds with argillo-calcareons concretions, of all shapes and forms, which appear to iiave been formed by molecular attraction, since the deposition of the beds. On the New York side of the lake, it does not foi-m a continuous deposit from the head of the lake to its outlet, but interruptions occur where the older strata reach the lake shore. On the Vermont side, it covers a much ureater extent of surface, and reaches from the lake to the base of the Green Mountains, or from six to twelve miles. The heigiit above the level of the lake to which it extends, is about two hundred feet. This ancient sea occupied the Chainplain basin, and the Hud- son forming a continuous arm from the Gulf of St. Lawrence to the mouth of the Hudson, at New York. In 18U9, Prof. Charles T. Jacksonf mentioned a recent marine Tertiary deposit, at Augusta, Maine, eighty-two feet above the level of the Kennebec river, where it is said to form the substratum of a laro-o portion of the valley. Win. B. and Henry D. Rogers;]; described the Tertiary in the counties of Lancaster, Northumberland, Richmond, Westmoreland, King George, and the eastern part of Stafford, in Virginia; thus in- cluding the peninsula between the Potomac and Rappahannock rivers. This area forms the northern portion of the Tertiary of Virginia. The Miocene extends from near the l)ay shore, westward over the larger portion of the peninsula, while the Eocene occupies the remain- ing area on the west. Tliev dcscril)ed from the Miocene, Tnrr/.teUa Jtvxionalis and Fasciolarin rhomhoidea; and from the Eocene. Cytherea lenficiilan's, now Dosiiiiop.sis /eiif/cidaris, CrassatelUi capri- cranium, Cucullnea ononcheila, now Latiarca ononcheila, C. trans- versa, now L. transversa and Venericardia ascia. * Geo. Rep. N. Y., 18:58. i Third Annual Rep. (Jco. of Maine. I Trans. Am. Phil. Soc, vol. vi. ~ Mesozoir, and CUmozoic Oeolofjy and P(il(vontlineafnm,, Cardita abbrcriata, Pecfnnrnlus raroJinensis, and /*. arafns. Prof. Emmons** found the direction of the drift scratches and scor- ings of rock, in the eastern i)art of New York, confoiniing to that of '■" .Tour. .\('!iil. Xiit. Sci., vol. viii.. pt. 1. t Am. .four. Sci. and Art.', vol. x.x.xix. 1 (ifo. Siir. (if l)('!:nv;ir(', ISJI. I (ico. ot'.MMSHiiclmsctts, IMl. II Am. .Tour. Si-i. ;iii(l Arts, vol. xi. IT Am. .Tour. Sci. innl Arts, vol. xli. ■■* Geo. 2dDist.X. Y., 1812. 160 Tertiary. the great vallc\'s. In tlio Oliuinphiin vallov, it is nearly nortli and soiitli; and in tiie St. Lawrenee valley, nortlusast and southwest. The marine Tertiary of Cluiuiplain, tliongh deposited in quiet waters, al- ways overlies the scored and grooved surfaces. The l)owlders succeed this Tertiary or are mixed with it. It is mineralogicaily composed in as- cending order, of first, a stilf blue clay; second, a yellowish l)r()wn eiav an d third, a yellowisli brown sand. The second o\ves its color to weathering rather than to any important dillereiice in its composi- tion from the lower clay. Sand begins to ajqx.'ar in tlio yellowish clay, and increases gradually until it predomimitcs, and finally becomes a pui'C siliceous fiand. No fossils liail then l)i'en discovered in the clay, but in the clay and sand and upper part of the group fossils are I'onnd as if in llieir native habitat, exceedingly frail, preserving their mark ings and edges entire, forbidding the idea that they could have been drifted into tlu.'ir present position. In protected places, as at Port Kent and iJeaitport, the thickness of th.; group is aliout 100 I'eet. In unprotected |)laces, the larger part of the group has been swept away. (commencing at Whitehall, at the head of Lake Champlain, it may lie traced continuously not only the entire length of the lake, but also to Quebec and far toward the Gulf of St. I.nwrence. It lines the St. Lawrence river as fitras Ogdensburg. And from AVhitehall south it linvs the Hudson river for a long distance. The Albany chi}' belongs to this group, and is therefore one of the most recent of our marine formations. Ml', ('onrad* described, from the "Miocene at Calvert Clili's, IMary- land, J'cnus latiUratd, tUjiherea sohnasutu, Lvcina forcnuDit, L. xnb- plditd/d, Cardiu)!/ leptopleura, Astarle rcriciis, A. exaliafo, Liin(( papyrid, Area t^nbroslrdtd^ Pleiir()lo}iin, TrovJitis perdlve(((iis, SadnrUi pdchyplenrc, Sohiriitm fri/l'icddon, now Arvhitcctoiiica IriUneala^ Iir/'ioidibu/inii perarmtitum, Flssurellc mdri/hiinlicfi, Dispola'.a rainotid, Cditcelldrid bij)lic/'J'erd, C enyoiidtd, BditdUd h'liedtd, Tarritelld indentd, T.cxdltutd, T. perlaqueata, Jf<(r- giiieJ/d prrexHjud. And also Astrea maryldndicd, incrusting Pec!,en madisoiu'iis on James river, Virginia; A. he/lc, from Newbern, North Caroli n;i (kirdiioii nicu/letti, now Protocardid nlcuUetfi, (rom the Lower Tertiary or Jackson Group, on the Washita river, Monroe county, Louisian;i; and Fii;,ii.i pdchylciirns, from the Lower Tertiary of Alal )aina. Edmund Ravenel| described, from a Pliocene calcareous deposit on Jdiir. Acail. Js'at. Sci., vol. viii., iit 2. t yiy''l. Meso.~oi.(- and Cijfini\ and IVom the Jackson Grou}), Anouu'd ji'i/osa.. lie said, tliat in a ^i'w hours' examination of the Afiocene marl, in the vicinity of Petersburo; Ya., he was enabled to collect about 100 distinct species. This locality is the western limit of the Miocene, winch is here based on gM-anite, and is the spot, in which, to search for the estu- ary and fresh water shells of the Miocene pei'iod. The elevation is considerably more than 100 feet above tide, and as the rise decreases toward the sea, it is probable that the primary rocks continued to be U[)lifted even after the era of the Miocene; indeed, how c;in we otherwise account for the elevation of fossiliferous beds, even of those of the Post-i)liocene period. It is an interesting- fact that the Miocene estuaries were inhabited by two species of bivalves, now extinct, of the same two genera which still occur in similar situations in Florida and Alabama, that is at the conlluence of rivers and bays, where the water is nearly fresh. These genera are Gnathodon and Cyrena, both of the family Oj/i'eni'die. The extinct Gnathodon has a considerable I'escmblance to the recent species, but the Cyrena is widely different from the living shell. These .,,;,( v|* * Proc. Aoiitl. Nat. Sci., vol. i. T^P fX 1G2 Terfiorii. Ibsnils ;ir(' froqiuMilly WiitcM'-woni, always with disunitod valves, a\ul appear to have hopii transported. Occasionally a specimen occurs not in the least abraded, a circumstance which indicates th(> vicinity of tlie Petersl)ur<4' deposits to the mouth of the river. The strata occur in a meadow, and consist of blue marl, of a sandy texture, often inter- mixed with small gravel and ferruginous sand, full of shells ; there is here also a proportion of gravel, of rounded quartz, occasionally of hirgo size. Water- worn fragments of bivalves are abundantly inter- mingled with entire shells, and many species occur with connected valves. 'I'his is particularly the case with the burrowing shells, as Pa)i(>p(i:f(, but also, though less frequently, with the large Venus tri- dactioidcs, Crassute/la undiilata, Asfarfe concenfrica, Cytherea al- harld, two species of (Hifona, and even two spe(!ies of Ostrea are not uncommon; but there is nothing like an oyster bed in these stjata which might indicate shoal water. 'J'he i)ro|)ortion of oysters to the other bivalves is about the same which the dredge furnished at the mouth of Ca[)e P'ear river, North Carolina, at the depth of eight fathoms. In 1844, Prof. J. W. Bailey* identified numerous living Infusorial forms with the fossil Infusoria, from the Miocene at Petersburg, Va., and Piscataway, ]N[d., and described several new species. Mr. Conradf described, from the Miocene, at Petersburg, Va., (Jrepi- duhi c;/mha!formi.s ; from the Eocene at Marlbourne, Hanovor count}'. Va., Cijtherea erersa, C. liciata, C. subimpressa; from Stafford count}', Va,, C. P!i(i(( ; from Claiborne, Ala., Cardita densata ; and from near Santee, South Carolina, Pecien elLratAis. Dr. Edmund Ravenel described, fiom the Miocene of South Carolina, Pecfen morfoiif, ; from the Eocene, Terehratidd canipcs, and Scutella, pileiissinensis, now Mortonia pilenssinensis. And Dr. Robert W. Gibbes described, from a bed of green sand near the Santee canal, and about three miles from the head waters of Cooi)er river. South Carolina, Dorudo)) sc.j'i'aftis'.'l In 1845, Prof. James Ilall^ described, from Tertiary, slaty, bitumin ous limestone, on the dividing ridge between the waters of Mudily river flowing eastward, and those of iNIuddy creek flowing into Bear river on the west, in long. Ill deg., lat. 40 deg., 3fya fellinoides, ''■' \m. Jour. Sci. iinil Arts, vol. xlvi. t I'roc. Aciul. Niit. Sci., vol. ii. t 'riiis species was erroiuously meutioneil as Cretaceous on page 15, vol. iii,. of this .lounial, or page 51 of this article. 5 Fremont's Kxpl. Exped. 3Icsoz(>/'(' and flcBnozni'c Qcoloffi/ mid P<(hvonfolo(j!). IG:^ now Unio fellinoidcs, PlenyofonKiria inu'unyidafn^ (■erifhiinii frctnoiiH, C. tcneram, now Gotiiobasis fetiard, Natica (?) OGcfdenfnlis, and Tur- bo jxdndhmfot'mis, now Viiu'/xn'Hs palKdiud'/onnis. Willi.'ini Lonsdale* (lescril)od, from the MioeiMi > of Virginia, (Udmn- naria sexrffdiatd, ITctevopora foi'fil/s, now Jlidticrescis tortiiis, Es- ch'irfiin ti(midi(hf,\ui\Y Cellcpora f nmldnht ^Cquadra ii(iHl(iris,\\o\\ Eep- focxlleporarin qtixdrniirftdan's, (J. hifoviudfa, now li. itiformata, ^ '. ■simllis, now R. slmllh, C umbiUcnta, now MuUiporind Kinbilicatd. From the Edccmo, Ocellaria ramo.sa, Fl(dteiln}ii, ciDiei/orme, Dcndro- phyJIia J(i'vi,s, ('l((docer<( recresceihs, ddryophjilliti siihdicholomd, Id)iio- nea comin/srens, T. niaxUhirh, IlippoUioa iiiberculum, now Pyrijlns- trella tubercnii'^ Eschard iticumbens, E. j^etiob's, E. tubiddtd, E. vlmmea, E. lined, now KsrlidriiKdld lined, Lnnidifcx distans, L. sex- dii(jiddft/s, and L. c(jiiH(/inis. Lycll and Soweihy doscrihcd Terchrd- fidd ioilini)}(/toi}ei).sis, now Jihijnchouelld ivi/)iiiii(jfoiiei)sis, anfi. and Arts, i!il scr., vol. i. t Am. .four. Sci. und Arts, id ser., vol. ii. 'i I'roc. Aeiid. Nat. Sci., voi. I'ii. mw 104 Terfidry. #11 It was foimd bonciilli Llie fossil hones ol' {.\w Me(/(i/oiii/.,',ji>/l'ers()i//\ and Mastodon (fi(/fni leinn. In J847, W. Vj. Lo<4!Hi* (bmK'l niariiio tostacoa alony the valley of tlio Ottawa, ill llie clays and sands thai form tli(> siipf rficial deposits. These dci)osits eover the wliolo valley of the south Petite Xatioiiand its triI)Mtaries ; and occur in Teniph.'ton, Hull, Xepeaii, raciu-i.hani, and Filzroy, to the mouth of the Mississii)[»i ai.d Madawaska, They were found in Fitzroy. iJIJO feet al)ovc the level of the sea, and in Nepeaii, -110 feet above the sea, where Sa.c/cfira nuiasd occurs in the g-rav(>l. At the mouth of Gattineau, ueai- IJytown, not only mai-ine shells were discovered, but in nodules of indurated clay the Jfullofjrs villosi/s, or common ca[)eling, a small (ish, which still frequents the shores of the Gnif of St. Lawrence, was obtained in vast nun)I)ers. CIrooves aifd scratches on tlie surfaces of the rocks were met with on the Gattineau, between Farmer's and r.lasdelTs mills, liavinj;- a direc- tion S. I'Ap E ; on Glen's creek in I'ackenham, N. and S. ; on the Alln- mettes Lake, at iNIontgomery's clearino-, S. 25° E. The shores of Lake Teiniscamang, which is lon^- and narrow, and has banks bold and rocky, rise into hills '200 to 400, and sometimes 500 fet^t above its surface. The general valley of the lake thus bounded presents several gentle turns, the dii'ections connected with two of which, reaching down to the mouth of the Keepawa. river (35 miles), are 158°, 101°, 15(5° numbering the degrees from north as zero around by east. The parallel grooves in these reaches of the valU'y turn precisely with them, as if the bounds of the valley had been the guiding cause of their bearings, and they are registered on various rounded and polished surfaces projecting into the lake, and sometimes rising to 30 and 40 feet over its level. These projecting points did not dellect the gi'ooved lines in the slighest degree. In one case, where the projecting point is 35 feet high, the furrows were ob- served to move over it without an}* deflection whatever ; so that, what- ever botly, moving downward in the valley, may have caused the grooves, it was not deflected by meeting an obstacle 35 feet higher than tlie surface of the lake. On die top of this projecting point, the grooves are crossed by another pai'allel set at an angle of 15°. The C)ompany's Post stands on a point on the east side, which cuts the lake nearly' in two, at about 18 miles from the head, and it is oppo- site a less prominent point on the other side. These points approach to within a (juarter of a mile of one another. Both are composed of * Geo. Si(r. Can. Mesozoic 071(7 (Uvnozoic Geoloiji/ anil I'dhnontolofjy. ir.r, sand Mild !^TiiV('l, wliidi, on tlu; cast, tonii a liill l-'U) feet lii^li. TIk' soutlu'rii fai'o of tliis hill riiiiH in tlu> bcarinu," (5,')°, ami the yravcl \n- Avard the eastward rests on flat sandstone strata, which have a sii.ootli and partially rounded surCact'. The gravel and the rock constiintc the north siiU'ol'a dee}) hay. The ii()lislie(l rock surface exhiliils wdl iiiarkeil Lii'oovcs, which come IVoiii beneath the uraxcl hill, nearly at ri<>'ht annles to the maiLiin of the water. 'I'lierc; is here, as in some otlier instances, more than one set of parallel scratches. Two of these sets cross one anothci- in the directions 110° ;iiid lUO^. \n the eastcni bay, at the head of the lake, near the moulh of thcOttei- river, paiallcl groo\'es were remarked riinuinii in the luariiru' Id")", which is tlicu[)- ward direction of the valley of that stream; and about ;i mile west- ward of the IJlanciie, in the sann; bay, in the bearing' I'lO^, partakinuf of tiu,' direction of the v.'iUey, bounded by the escaipmeiit n[' the limestone described as runiiinn,- l)ack into the interior. On the cast siile of the lak(>. three liowlders were reinarkcil, which had been moved by the ice the previous winter. One of them measiiriuLi' .'!2 cubic feet, li:id been nu)Ved nine feet in the (liiection 00'^; ;iiif>tlier lOO cubic feet, had been moved twelv(^ feet in the direction ll'AP; another 80 cubic feet, had been moved I i feet in the direction :i")()°; each had left Ix'hind it a deep, broad fui'i'ow throuji;h the liravel of the beach down to the clay beneath. In front ol the lirst was accumnlated a heap of <2,ravel, one foot hinli, with an area of!) square fecst; in fVont of the second was an accumuiation of small i)o'vlders wei<;hing from SO to lO'i lbs. each. To move the second and third, the [troiiress of tin.' ic(! must have Iiccn up the lake, and tin? first across it. Had tin; t!,i;i\el rested on the surface of a rock instead of ela\', parallel scratches would have l)ecn the result in each ease. Thei'e ar(> deej), water-worn holes on Mio banks of the Ottawa, at liciuhts considerably above the highest level it has ever i)een known to attain. One of these, 18 inches in diametei-, near Chenaux, is GO feet above the existing surface of the water; another, on the island at Por- tage Dufort, 2e5 feet above the water, and I'i oi- l,'} feet over the great flood of the preceding spring, is more than ;") feet deej), measuring 2 by 2|- feet in diameter. Alexander ^Murray found Tertiary deposits on the eastern pc^ninsula of the Province, between the Bay Chaleur and the (lulf of St. J.aw- renee, consisting of clay, generally of a bine color, with sand or gravel over it, and forming the banks at the mouths of the riv(n's. Over the ■clay in some cases, as at the mouth of the Chat, marine sliells were found deposited in layers, MO feet above high-water mark. At the "i"i| I !^ ICO Tei'linry. 1 ♦'■,! i I' I I '1. month of tlio Mjitan the clay and gravel IxuikH nro npwnrd of SO fet't lii', crossing the Saluda and Broad rivers, near their junction; the Wateroe, at the canal; Lynch's creek at Evan's Ferry; and Thompson's creek, at the point where it enters the State, in Ches- terlield district, will approximately maik the northern l)oundary. Wherever the rivers, in their downward course, entoi- this bonndary, they wash away the more yielding Tortiar\' rocks, aulrict. The protectcil patches may be tr;,cc(l, at short intervals, from Ilorry to I)arlin' the coast of al)out S or !) niilc.^ in breadth. The fossils are nearly all re- ferable to livinjf s[)ecies now inhabiting the coast ; a few, however, belong to the fauna of Florida and the West Indies. There appears to have been a sliglit ilc\;ition of the coast during this jicriod. T. A. Conrad''' separated the Eocene into tin; Ui)per or Newer Eocene, found at Vicksbnrg, Miss., and including the white limestone of St. Stei)hens, and of Claiborne, Ala., and i)art of that in Charleston county, South Carolina, cliaracterizcd l)y Scutella li/elli, S. royci'si^ Peafen poKhonl, and Ninntnnlites maiifelli; and the limestone in the vicinity of Tami)a ba.\', Florida, charactcri;ced i)v NiimvKilites Jloridnna^ Cria- tclJaria rote/la, and Ostrea (jcoryiana ; and into the Lowe' or Older Eocene, consisting of the fossiliferons sands of Claiborne, and St. Stephens, Ala., of the Washita river, near Monroe, La. ; of I'amunk}' river, at JMarlborne, and the greensand on James river, below Cit}' Point, Va., and at Fort Washington, Piscataway, anil Uppci Marl- borough, ^Laryland, characterized by CarditK phoii'costa, C. hlan- dinyi, Cnoisotelld ■ 't<(, Ostrea sellivfoDuis, and Tarn'feJht mor- loni. He described,* from the Eocene, in the vicinity of Vicksbnrg', Mississippi, Den' Hum mississii^piense^ FissunMa mis- '■' Proc. Acad. Nat. Sci., vol. iii 168 To'Uiii'ij, Kt'fisipji/ensis, Soffirivin h'iln'ahtm. now Arrhft.ectoin'oa trUirnta^ linlhi ('t'dssi/if/iut, ('j/j)t'(i(i sjthd i'oith'.H, ('. //'tifcK, S'tiriro tiu'ssis.si/>/iiciisfii, Sif/arc/its )tn'ssiNfi)l(iisln^ .V. n'i'h\slniriiensin, Scjtlnrid tihihifimo'id, 'I'uvrilvllc nii.isis.'i//ijn'nife, P.rnlmlcns, I', .scvi'iihnn, /'. fnntnluin, I', tciielhtni, I'liorns /iiiinilin, Bucciiinm mi.ssi.sfiijipieiise, 'J'jiphls cin'riro,s/i'iM, Mwcx mi.ssi.sni/)}n'ctiniH, Mc/oiH/OKi i-rnssfconiiifii, Fiisiis viississ/p/tioisi's, now Ficn/isis mis- ni.'dpijn'.d, now G. pdpijrid^ Crds.sdfc/hi 7)n'.siii.ssij}picnNis, Cnrd/nm evci'sum, C. dircrninn, now Proli)('d}'did dirersd, C. i'icA'Nhin'ifeiine, Tellina pectorosa^ T. ncricd^ T. vickubin'ffcnNis, Donaxfnnerahi, Cythd'ea d.shn'/i/on/iis, C. imitdbiUs C missi.s.sijipicnsis, C, sobrina, C. perbrcvis, Corbis nhimiiicd, Luc/iid miss/Ksippiensis, L. perlceviti, Loripes ebvrnca, L. tnrr/ida, L'orbnld nlfa, C. ciii/iDidta, O. interstrinfu, C/iatiid misfiissipjiienb'is, Pectuncidus arctdluH, Nuevld sericea, iV. ricksbiinjenfiis. Area mississippiensi.s^ III/ SSI Id red h'rnd.^ JJ. nii'ssissipp/ensis, B. protracta, Avicida arijenfed, Modiohi nu'ssissi'piensis, now l^olsclla mississippiensis, Pinna dri/enfed, Lima shuninea^ Qstrea vicksburr/ensis, Phohis friquetra^ Jlddrepora mis.sissipieiisis, M. vicksbiirr/ohsis, Tnrbinolia cdulifera^ now Osleodes canh'Jeriis, Lnnulites vicksburijensis, now OUijoiresiinn cicksburf/ense. From ihe Eocene, at Claiborne, Ahibanui, and other places, AinpuUdrin (?) perovdht, Tnrbinolia elahurahi, now Osteodes ekiboratus, Jlddre- pora rennicnlosd, now TJcudropIii//lid vcrmiridosa : and from St. Matthews Parish, Orang'eburg District, Sonth Carolina, NucAda calcar- ensis, JV. carolinensis, Cardita bilinedhi, C. cdroh'nensis, C. vigintindrid, C subqiiddraht, G. siibrotiinda. Turbo bilirdtns, Ccri- t.hiuin siliceiim, C. bicostellatiim, Tnfnndibuhim cdvindhim, Tellina siiboiqiidlis, 3fadrepora puiwtalata, Naalilopsis vanuxemi. From the JIcsu.~oi<: (tad t'picii}iis, now (inri niisstssippfiiiisiK, From the ( .'oluniliia river, f near Astoria, Xnriilti nhviiptii, y. ci'iicij'onin'n, N. (Ih'iii'lciihi, .V. pntlUi, Miirtrn ullmi'in^ 'J'clliiin oi'f'i/ttneiisis, T. abriifj', Loripas pnrills, Soh'ii ein'his, ('i///i>re)n. Dr. S. (1. Morion dcsciluMl, I'rom tlu; Eoi-cm! of WaHJiinyton t-onnly, Alal)ama, Cfdnris nlifviniciisis, and d'tihri/cs ayastilrzi. And Dr. Rohi-rt \V. (iil)l)os di'S('ril)L'd, from the K(»('('n(! of South Carolina, ('iirchcrodon morfoin, 0. (fciifidciis, (.'. liiii''i/'i>i'ini.'i, Oxijrhiiifi ■siUiitKUii. Otodi's Utvis^ and (iliiphis suhtddtri. In 181!), T. A. Conrad.:< doscriljiMl, from the Up[)er Eoeeno of Vicks- bnri>', ^^Iissis,sii)pi, ('lare/ld vicksburyctisi.s. now Fasciolaria vickshurii- cnsls, Fidi/nr nodiddtinn, and Ti'ihm HdhuU'enfiis. And l{ol)ci't W. Gil)l)os described, from the pjoeene of South (,'aroiina, Gcdeocerdu con- torfii.s', and Oxf/rhina wihonl. In 1H.")0, W. E. Lo<;;ui| said that in tlic valleys of the Gonlfre and the Mnrray Uay rivers, as well iis along the mar<;in of tin? St. Law- rcnee between them, tb.evc are, at various parts, great acenmnlationsof clay and sand, witi; some gravel; and it is very perceptible that while they ol'ten present a ccr.risi.! aggregation of hnmmocksin the lower grounds, at liigh^r 1( 'Is. '.in- in horixontal beds, tiiey are ari'anged into a succession of .'ijjK^siie t . .-.•aces of ecjnal lieight along the sides of th(^ valleys, and 't !',.^!on(Ii! erraces at intervals along tlie St. Law- rence, all probably \\iuvwif:f uiicicnt l)eaehes or periods of retrocession of a Tertiary sea by the elevation of tlie land. One of these terraces, in the valley of tlie Gouffi'e, has a heiglit, as indieated by a s[)irit level, of DiO ftv.t above the Bay St. Paul, and another lias a height of oGO feet. * Jour. Acad. Nat. Sci., 2(1 ser., vol. i. i Am. Jour. Sei. and Arts, 2d ser., vol. v. I Proc. Acad. Nat. Sci., vols. iii. and iv. § Jour. Acad. Nat. Sci., 2d ser., vol. 1. II Guo. Bur. of Canada. .,,,,jf ^^PPM no Tertiary. ■ ( Tlie deposits in which these terraces have I^een worn consist of clay, containing- marine sliells, among which are Telllan groenlandicM, T. calcared, Snxicavd riujuso, NnGiihi, Venus, 31 ij til us, and Ba Janus. These shells were I'onnd as high as lUJO feet jibove the b-iy. At Little Malbide there are six terraces, plainly- distinguishable, one above another. T. A. Convad* described, from the Eocene of Geoi'gia, Mifra geor(iiana, Catopygus conradi, now Cassuhihis conradi, Ilolnster mortom\ NucAeolites hjelli.^ Discoidea haJdeuKiiii, and Cidaritcs wortonl. Robert W. Gibbes described, from the Eocene of Asjiluy river, Mulichates holmesi. And Zadock Tiionipsonf described, fron) the drift in Vermont, exposed in excavating for the IJutinru and Burlington railroad, Delphinvs vermoutavns, now JJchir/a vt:r7ncn- tona. In 18")], Philip T. T^'son;}; described the Sacramento Valley as along prairie, occupying the space between the flanks of the Sierrt. Nevada and those of the Coast Range, closed in on the nortl; by the terminal spurs of tiie Cascade mountains, iuid on the south by th'; junction of the Coast Range with the Sierra Nevada. Its gieatei^. , width is less than 60 miles, but it maintains a mean width of nearly 50 miles throughout almost its entire length. The surface strata ar^ not older than the Eocene or Miocene, and rest immediately ui)on the metamorphic and hypogene rocks. Trof. James Robb^ showed tlie direction of the Dril't striip in New Brunswick to be, generally, about 10 deg. W. of true north to 10 deg Fi. ot so\ith, but that some stria' have a direction N. ;!0deg. E. Others N. 45 deg. W., and still others east and west. T. T. Bouve|| described, from tlie Eocene of Georgia, CatopijfiKs pa- telliformis, now Cdssulidii.s pafellifornu's, and Ilemiasier conradi. In 185'2, Mr. J. E ,'ans^| exploi-ed that region of the I'pper ^Missouri country, lyiug high upon White river, called the '^ Maura isvs Torres''' or "Bad Lands." He said that from the high prairies, which rise in the back, by a series of terraces or benches toward the spurs of the Rocky Mountains, the traveler looks down into an extensive valley, that may be said to constitute a world of its own, and which appears to have been formed partly by an extensive vertical fault, and partly by the long continued influence of the scooping action of denudation. * Jour. Acad. Nat. ScL, 2(1 ser., vol. ii. T Am. Jour. Sci. and Arts, id ser., vol. ix. t (iL'o. and Ind. Kesoiirci's oi'Cal. ij Proe. Am. Ai^s. Ad. 8oi., 4tli Mooting. i Proe. IJost. Soe. Nat. Hist., vol. iv. ir 'ieo. iSur., Wis., Iowa and Minn. Mesozoic atid Cnnozoic Geolo(]ij (did P(thvont(ilo;iy, 171 o\v The widtli of this vnlley may be about 30 miles, ami its whole ]i'ii<>tli about 90. as it stretches away westwardiy toward tlu; l)aso of the gloomy and dark range of mountains known as the lilaek Ilili-^. Its most depressed portion, 300 feet below the general level oftlm surround- ing country, is clothed with scanty grassc-'. and covered by a soil similai" to that of the higher ground. To the surrounding country, hnwevei", the IMauvaiscs Terix's present the most striking contrast. From the uniform, monotonous, open pi'airie, the ti'uveler suddeuly descends, one or two hundrcul feet, into a valley that looks as if it had suidc away from the surrounding world, leaving, standing all over it, thousands of abrupt, irregular, i>i'ismatic, juid columnar masses, frequently capj:ed with irregidar pyramids, and stretching up to a height of from one to two hundi'e(l feet oi' nu)re. So thickly are these natural towers studded over the surface of this extraordinary region, that the traveler threads his way through deep, confiried, labyrinthine passages, nut unlike the nai'row, irregular streets and lanes of some quaint, old town of the Euro[)ean continent. Viewed in the distance, indeed, these rocky piles, in their endless succession, assume the appearance of massive, artificial structures, decked out with all the accessories of buttress and turret, arched doorway and clustered shaft, pinnacle, and lluial and tai)ering spire. One might almost imagine oneself approaching some magnificent city of the dead, where the labor and the genius of forgotten nations had left behind them a multitude of monuments of art and skill. On descending from the iieights, however, and proceetling to thread this vast labyrinth, and inspect, in detail, its deep, intricate recesses, the realities of ti:e scene soon dissipate the delusions of the distance. The Ccistellated forms, which fancy had conjured up have vanished; and around one, on ever^' side, is bleak and barren desolation. Then, too, if the exploration be made in midsummer, the scorching rays of the sun, pouring down in the hundi'cd defiles that conduct the wa}' fa rcr through this pathless waste, are refiected back from the white or ash colored walls that rise around, unurtigated by a l.u'eath of air, or the shelter of a solitary shrub. The drooping spirits of the scorcl'cd geologist ar»' n<'t permittetl, however, to flag. The fossil treasures of the way, we!, repay its sul- triness and fatigue. At every step, objects of tlie highest interest present themselves. Embedded in the debi'is, lie strewn, in the greatest profusion, organic relics of extinct animals. All speak of a vast fresh water deposit of the early Tertiary period, and disclose the former existence of ujost remarka])le races that ro.-imed ;dn)ut in by- 172 Tertiary. gone ngos high up in the vallov' of the Missouri, toward the source of its western tributaries, where now pasture the big - horned Oois montana, the shaggy buffalo, or American bison, and the elegant and slenderly constructed antelope. A section oi' the Tei'tiary of the "Bad lands," or, " Mauvaises Terres," in ulMilv ns- soeiated with isolated Ueds of gravel ;jiid sand, among which great quantities of marine siiells of comparatively recent origin occui'. One of these localities is ou the Prescott Ixoad, aooiit a mile and a half from K('m])tville, wiiei'e a va-^l accnmnlat ion of TcJlliui (fixenhoidica oM'iiays a two feet l»ed of limestone gravel, the latter I'csting on gravc^l of a still coarser quality, and of more angular fragments, and irregularly mixed up with sand ami clay, some of the boivlders being from 6 to 10 inches in diameter. The height of this locality is about '550 feet over Lake St. Pester. Atanotlicr hjcidity, near Armstrong's Mills, the shells consist chiclly of xS'(/.t;<'c'(/(,"« n((/osa, mixed with sand and loam, at a height of about IIOO feet al)ove Lake St. T*eter. In Kenyon, on the Garry river, these shells occur at the height of 270 feet aViove Lake St. Peter. On the road between tin; r)th and 0th concessions of I'.ie towushi[). on tiie IDtli and tin; 21st lots, these shells occur at the height of 'MV) or •! 10 f(!et above Lake 8t. Petei'. Two localities occur in Locliiel. one; of them on the loth lot of the 1st concession, at the height of 201 feiit, and the other on the ->th lot of the same concession, 2S0 or 290 feet above Lake St. Pelei-, where the marine shells are mixed with the sand, and where Ijowlders and fragments of limestone and sandstone abound. Prof. Edward Hitchcock* described th(- brown coal deposit in Bran- e; and some of them liave been carried round its eastern eml, and now lie on the shores of Londonderry and Onslow. So, also, while immense numbers of bowlders h.'sve l)een scattered over the south coast from the uranite and quartz rock ridges, immediately inland, many have (b'ifted in the opposite direction, and may be found scattered over the counties of Sydney, Pictou and Colchester. The&e fact? show that the transport of traveled blocks, though it may have been |)rincii)ally from the northward, has, by no means been exclusively so; bowlders having lieen cai'ried in various directions, and more especially from the more elevated and rocky districts to the lower grounds in their vicinity. The surface of the coun.try was greatly modified by the drift; the ridges of Cumberland, the deep valleys of Cornwallis nnd Annapolis, the great gorges crossing ^he Cobequid mountains, and the western end of the North mountains in Annapolis and Digby counties, such eminences a?^ the Greenhill in Pictou county, and Onslow mountain in Colchester, are due in great part to the removal of soft rocks by d<;- nuding agencies of this jx'riod, while the harder rocks remained in pro- jecting ridges. The surface of the rocks are frecpiently found polished, scratched or striated. The striie at different jjlaees have different courses, and sometimes they are found to cross each other as at Gore mountain, where one set is S. (5.5 deg. E., and the other S. 20 deg. E. At Gay's river, Musciuodoboit Harboi-, and near Guyslioro the direction is from S. to X. At Poison's L:ike, from N. to S., and near Pictou, E. ct W. Bo.viders or traveled stones are off^n found in i)laces where there is no other drift. For example, on bare granite hills, about 500 feet in height, near the St. Mary's i-iver. there are large, angular blocks of quartzite, derived from tiie ridges of that inatei-ial which abound in the district, but are separated from the hills on whicii the fragments lie liv deep valleys. The only evidence of organic life during the ])owlder period, or im- mediately before it, noticed V)v Dr. Dawson, consists of a hardened, peaty bed, which appears under the bowlder cia\ on the northwest aim of the River of Inhabitants. It rests upon gray clay, similar to that which underlies peat bogs, and is oveilaid by nearly twenty feet of bowlder clay. Pressure has rendered it nearly as hard as? coal, thouah it is somewhai tougher and more earthy than good coal. It has a glossy appearance when rubbed or scratched with a knife, burns with considerable flame, and api)roaches in its chaiacters to the brown 176 Tertiary. coals, or more iinperfoci varieties of bitimiinons coal. It contains many small roots and branclios, apparently of on iferrius irces Hied to the spruces. The vegetable mutter composiiii-" this bed, iiust have flourished before the drift was spread over the province, so that it be- longs to some i)art of the great Tertiary group of rocks, of which the drilt is the latest member. Dr. Dawson accounted for the drift phenomena of Nova Sc-otia, in this manner. Let us suppose the surfiice of the province, while its projecting I'ooks. were uncovered by surface deposits, exposed for many successive centuries to the action of alternate frosts and thaws — the whole of the untraveled drift migiit have been accumulated on its surface. Let it then be slowly submerged, until its iiill-tops should become ishmds or reefs of rocks in a sea loaded in winter and spring with drift ice, floated along by currents, which, like the present Arctic current, woidd set from N. E. to S. W., with various modifications produced b}'^ local causes. We have, in these causes, ample means for accounting for the whole of the appearances, including the traveled blocks and the scratched and polished rock surfaces. 'V\\e sfratifled sand and (jravel rests upon and is newer than the un- stratilied drift. This may often be seen in coast sections or river banks, and occasionally in road-cuttings. In I'ictou county there oc- curs a very thick bed of conglomerate, of the age of the Coal Measures, the outcrop of which, owing to its comparative hardness and great mass, forms a high ridge extending from the hill behind New Glasgow, across the East and Middle rivers, and along the south side of the West river, ;.nd then crossing the West river reappears in Rogers Hill. The valleys of these three rivers have been cut through this bed, and the material thus removed has been heaped up in hillocks and beds of gravel, along the sides of the streams, on the side toward which the vyater now flows, which happens to be the north and northeast. Accord- ingly, along the course of the Albion Mines railway, and tiie lower parts of the INIiddle and West rivers, these gravel beds are everywhere »;xposed in the road-cuttings, and may in some plai-es be seen to rest on the bowlder-clay, showing that the cutting of these valleys was completed after the drift was produced. The stratilied gravels do not, like the older drift, form a continuous sheet spreading over the surface. They occur in mounds, and long ridges, sometimes extjcnding for miles over the country. They are supposed to have been distributed when the country was being elevated, while the bowlder drift was deposited when the land was subsiding beneath the sea. T.. A. Conrad separated the Eocene of Mississippi and Alabama, in Mesozoic and Cwnozoic Qeology and Paloiotitologi/. 177 ascending onlor, into : 1. (Maiborno group, (•hiiracterizcd by Cnrdifn denKOfa, Ostrea selliformis, Ci'dssdtelhi (ilia, PerfAincHhis sfam/'iiens, Merelrix auptiu'ea, Gro/elupfri hi/di, Leda C(i'/((f(t, und Crcpididft /irnfa. 2. Jac'ksdU group, eharactciizcd by Umbrella pldinilatd, Cardium nicollefUi\ Conns tortillfs, Ci/pratn fencsh'ah'.s, Gideodia pe/ersoni, and Rout ell aria exfenta. \\. St. StcpluMi's group, characterized by Pecten poulsoiii, and Orhitnliles indntelli. 4. Vicksburg group, cliaracterizcd by Corbnla (dfa, Crassafella m/ssissi'ppicnsis, Ai'c(( ^iiinsissippt'erisis, Merefri.r sobrina, M. fmilabilis,tin(\ Tin-blnella wihouL Tie di'scribed,* from Jackson. Miss., find Claiborne, Ala., Undopuc/ii/s expansam^ Ji\ triatujalare^ E. alt.icoHtatum^ Fhibdlnm wallesi^ Osfeodes irroratiis, Tiirbinolin luiudififormis, Chiloti , containing tlie remains of Infusoria and I'olythalamia, near ^Monterey, Caliibrnia. The strata are white, porous, light, resemble chalk, and are situated about two miles southeast from the center of Monterey, and form part of a hill which fronts the bay, and rises on the east side of the stage-road to San Francisco to the height of 500 or 000 feet. Tuoniey and Holmesf described, fiom the Pliocene of South Carolina, Celleporrt formosa, C. deprcssct, C. radio la, C. fessellala, 3Iembrani- pora lacinia, Plaeunanomia ph'cafa, Osfrea rarenelana, Janira cffint's, Pecten compari'h's, P. peedeensfs, Mi/f.ili(s injlatas. Area hlans, A. rustica, PecttDtcuUts lavis. Lniu'no cosf.ata^ Cra.ssafella g/bbesi, Psanimocola pliocenu, Dentalinm pliocenum. Ilipponix bidli, 3fono- donta kiaivahensis, Trochus armillatus^ T. f/enima, Terebellinn sfria- f,um, T. bnrdeni, T. eh'iranensi's, Volnfa frenholnn', Porcellana olioi- formis. Purpura tridentata, Cancellarift dcpressa, (J. f;enusta^ linsycon conradi, Cassidulus carolinensis, and Fasciotaria tuomeyi. J. McCrady described, from the same strata, Psavxniechinus exoletxs, Ayassizia porifera, Amphidetus amplijiorus, A. gntkicus, Jirissus spatiosKs, Playionottfs holniesi, and P. ravenelanus. Dr. Trask;|; described, from the Pliocene of Santa Barbara, California, Chenuiftzia papi'llosa^ Tornatella etlipfica^ Mvrex frayilis, Fusus bar- barensis, F. robustns, and F. ruyosus. * Proe. Aciul. Nat. Soi., vol. vii. t Tuoincy and Holmes' Fossils of South Carolina. 1 Proc. Cal. Acad. Sci., vol. i. w 178 Tertiary. '\ In 1856, W. P. Blak'i'" described the Tertiary rocks of the vicinity of San Francisco, California. They consist of fine-grained, compact sand- stone, associatcil witli shales, and underlie tlie city of San Francisco, and are exposed along the sliores of the bay, both noith and south of the city, forming the i)rinci[)Jil promontories and points, and several islands. On entering the bay fi'om the I'acifu', tiiey are iirst seen at Point Lobos, the cuter point, and again at North and Tonquin points. They border part of the Golden Gate on the north, and form the shores of Hichardson and Sancelito ba^ys. Angel, Yerba Buena and Alcatrazes Islands, ur(M)f the same age. In some places, hills and ridges of 200 or :K)0 feet in elevation are foiined entirely of this sandstone. Rocks of the sauK! age are found at Benicia, New Almaden, and between San Juan and Monterey. On the south end of the Island of Yerba Buena, a section, 200 feet thick, shows the sandstone layers, varying from a few inches to six and eight feet, ancl alternating with beds of argillaceous slates and shales. All the weathered surfaces ot this series of beds are of a rusty- brown or drab color, which extends throughout the rock to a depth of from ten to twenty feet, down to the limit of atmospheric influences. There are parts, however, of the u|)per beds that have not been reached and changed by decomi)osition ; these parts are found in the condition of spherical or ellipsoidal masses, from which the weathered parts scale off in successive crusts. These nuclei have the appearance of great, rounded bowlders, and have accumulated, in great numbers, at the base of the cliff. They are of various sizes, but are smallest in the upper parts of the strata, near to the surface. This spherical or globular condition does not appear to be the result of any peculiar arrangement of the material of the strata, a concretion- ar}' action, such as takes place in the igneous rocks, but is probably due to decomposition, the result of the absorption of infiltrating waters charged with imi)urities. A solid and homogeneous cube of sandstone thus exposed, under conditions favorable for al)sorption of the water on all its sides, would decompose most rai)idly on the angles, producing a succession of curved surfaces gradually approaching a sphere. The color of the sandstone is dark, bluish green, inclining to gray. It is exceedingly compact and tough, and does not break so readily as the fine-grained, red sandstone of the Connecticut river and New Jersey quarries. * Explorations and Surveys for a railroad from the Mississippi river to the Pacific ocean, vol. V. Jfesozoic (Did Camozoic Gcolofji/ and Pdhtonfohxjij. 179 A scn'tioii at Navy l'i)iiit, H.'iuciji, ox|)osoa a thicknoss of eoiiforin- ablt! beds of sainlstoiic coniiloincratc ami shales alittU; moro than 1,000 foot ill thickiu'ss. Tlic strata aio ii[)lil't('(l, hoiiii;- incliiu'd at an aiij^lo of tVdiii 20 to (50 (leu"., and dii)i)Uiy: toward tlu; soiitliwost. Tlif lii'iid of tlu' outcrops is 75 di';'. west of iioi'tli, and tiie strata iiiidcrlic, of rather form tlie liill iipo', which tlie governineiit huihliiigs are erei-tcd. The rid,L;e of coiig'lomerate is tii{> iiardest and most unyiehlin^' of all the strata, and its resistance to abrasion and atinosi»heric inlliicnces has determined tlie form of the hill and the sha|»e of Navy I'oint. It is prominent at several points, aloni^' the surface of tlie y llie iieicoL-itioii of iiiipiire waters; also, hy layers of the s;nne iii;j;i(Mlieiils, (I'Meriiiu' in tlieii- fineness, .'uid by oeeaslonal sejinis r»t oh;uc<);i!, ii, IVn^incnts. Thin layors of peldih's arc^ also nnnierons, even ••unoiiLi' th'' strata nl' the finest niateriais. Tlie ineliiieil stratilieatiMn, eaUeil (liiinon.-ii stnitili- cation, is viwy eoniiiion, and in many enses is heMiitifiilly siiown by iniiltitndes of the linest layers of sand, ineline(l in ditlereiit directions. He also idontilied tliis Grniii) on Chieo ei'tck, in the v;illey of the Saer:in;eu;o, Mt the foot of the Hills of the Sierra Xeviidii, on C'lrrizo creek, n(>ar Sjin Diego, at Williaiii'^on's I'.iss, f.os Aniielos and S;in Peib'o. Near Monterey it contains ji bed of microscopic oruMnisnis, 50 feet in thickness ; and li(> sii|)i)')s(!d it (o underlie the alhivinni of the ('ol()ra they are comi)ose(l in great part of Tertiary strata, thrown into great wave-likt' flexures, with here and there a gi'anitic axis of limiti'd extent, but with serpentine abund;int. In the auriferous regions, a similar s(!r|)i'ntine abounds, and has in all cases tlu! aspect of an intrusive rock. The movements which attended the uplift and plication of the Ooast Mountains, must have alU'cted the whole west(Mn sloi)o of the Sierra Nevada. He expressed the opin- ion that the impregnation of tlu; rocks with gold, and the formation of the (4)ast Mountains, were nearly synchronous. He descrilKHl, from the .Aliocene, at Point Lobos, near San Francisco. SculeJhi interltne((f(i, and from a l)rown calcareous sandstone at \'ol- cano Ridgi", Leda sulxw^iita^ now Niicnhinci .suhdciifd. Prof. Agassi/, described, iVom Ocoya creek, at the western base of the Sieri'a Nevada, Echinorhinufi hlnkci, Scymnns orcfdenfjdis, (rdlcocerdn prodiic/Ns, Pt'/()iiodo)i anHqiuis, Tlemipristls hetei'opleitrus, < 'arrhdyodon rerfas'. Oxijrhniii pJaiid, O. fnrnida, Lamna chivahi^ and L, orucUa, T. A. Conrail describiMl, from the same locality, JSTatira i/eiiiridafa, JV. ocoii- ana, JhiUajiKjnhin's, Pfeti.rofoiiia fraiisijtontaiinin, Si/cofijpiis ocojjdiiifn, Tarritella ocoijajio, doUis (irrtaf.as, Tellliid ocoyana, Meretrix decisa. Pec/en ncvudcus/.s, P. catilUforinis ; from the wSan Diego Mission, Curdlmn ^iiodestum, Corbiihi dfeyoftiia, Xitcnla dei'/'sa, 7\-l/iii(i dieyo- ana, T. congesta, Mactra dieyoana, Narica dieyoana, now Vunikor') Meno.ioir (iiiil (!iV)in)nsiriii, Tt'oi'hi'ta dliffotnxi ; (Voni .Monterey coiiiily, ('ij^litci'ii iiiilcs Hoiitli (>r Trc.-H I'iiiO"^, Mevclrix iniiomen's , IVitin llic 'I'lil.in' vmIIcv, Mereli'ij' fiilnrtind. Arrn int'crodoufd, piirjiin'o /je- frosii ; from (!;iniicll(), f,iifr(n'i(( fru.s/rci \ IVoui sixti'cn miles soiitli of 'I'rcs I'iiios, Modiohi i-oiih'ucht, ii(»\v Vnlsclhi ('(nifj'nctti; from ( 'urrizo Cr< t'lv, /'ccfcii (fcscr/i, mikI Os/rca hccriii'iini'. lie (Icscriltcil, iVoiii llic I'(»-;l |»li(>r('ii(' ;il S;iu I'cili'o, Tellhin jnd- t'omiii, Stixh'ord iihi'ii jifii ^ PoJi'li-(dii pidrmi ii( i. diiil C/drdi'iiln cdli/'oni icd. It is ([nite likely thai [)art or all of tin- strata referreil to the Fvx'ene from wliieh these fossils were collected, lieloni!,' t,o the ( 'retaceon^*. He de^eribed/'- from tlu' .Miocene, at Santa Barbara, California, Jdiiird helld. Mill In id deiisd/ii, Ai'cd eiDidlis, A. frilincald, Axiiiit'it bdrhdri'iiniH ; from Santa (Jiara, Schizo/)!/(fd edlifurnldiid : from Kstrel- la valley, Palliatii cslrclhiiiiim, now Lijropeefen esfrelldiiinii,S/)oiidi/liis eslrcllaiisis : from Monteicy county, Pdllimtt, nrdssicordo, now Ljiro- pecfcn enissicjjrdd, Tlirddd iiuicfropsin, -^fi/" iiioiifereijdnd^ Arcoi>d(iia niedidlix, Cnjptoniiid oi'dlis^ fijclns fefricd, Dosinia altd, I), loinjnld, Taiiiiosoiiid (ji'C(jd rid, Astroddpaia diUiselii ; from San Rai)hael Hills, Peetcii ineekl, P. dlliplicdhis ; from Santa Inez iNFountains, /'didn/- desnid iiiezanHiu ; from Kanelie Trinmpho, near Los Angi'los, Lnh'dria tfdHsuiDiiUind ; from other })laces in (yalifornin, Arod coutjestd^ Tapes liiilc.diinn ; and from Texas. Melliln Icxdna. Dr. Leidy described, tVoni llu- r>ad Lands of Nebraska, Hippdi'lon oceidentdle, now llippotheriiuii oi'i'identdle, II ijopoldiiiiia dineriediius, Lejddncheiiid deeoid, L. vidjor, Leptochixirus s/iecldbilis, Sleneojiber nebi'ftxccnsis, /.schi/roihi/s li/piis, Paheidnf/ns hdi/deir', Eumijs elci/dns, Aiiijdiii'ijon \ .i{/riocha')'iis nidjor, Enteledon ini/en.s, now EUdherlaia iiii/ens, Pdlwochnwus probiis, now Perehonrus probas ; "* I'roi'. Aead. Nat. Sei., vol. viii. ^, IMAGE EVALUATION TEST TARGET (MT-3) 7 Ss 7 f 9^ ^/ 1.0 ^^^ ^^^ Ui IM 12.2 It! U4 ■"■ 1.1 l*^ ^ ^ m L25 iU 11.6 Photographic Sciences Corporalion 23 WKST MAIN STRUT WEBSTER, N.Y. 14SS0 (716)872-^503 v**" i ¥ 182 '* r: *i((ry. 11 'I, 1/ i from Bear creek, Protomeryx hnlU ; from the riiocene of Ashley river, South Carolina, and from the Pliocene of New Jersey and Vircjinia, 3Ianntus f^ TTpiJor Tertiary' of the Bijou Hills, on the Upper jMissuuri, Ilerychippus insiynis, now Prof.ohippus inslynis and Leptarctns primus. In 1857, Dr F. V, Hayden* made an estimated vertical section, showing the order of superposition of the ditforent beds of the Bad Lands of White river, in Nebraska, referred to the Miocene, in ascend- ing order as follows: Bed A. — Light gray, calcareous grit, passing down into a stratum composed of an aggregate of rather coarse, granular quartz; underlaid by an asii-colored, argillaceous, indurated bed. with a greenish tinge. TtfanofJierium bed. Best developed at tlie entrance of the Basin from Bear creek. Seen also in the channel of White river. Tliickness, 50 feet. Bod B. — A reddish, fx-sli-colored, argillo-calcareous, indurated materi- al, passing down into a gray color, containing concretionar}' sandstone, sometimes an aggregate of angular grains of quartz, underlaid by a flesh colored, argillo calcareous, indurated stratum, containing a pro- fusion of mammalian and cheloniun remains. Turtle and Oreodon bed. Revealed on both sides of Wliite river and throughout the main body of the Bad Lands. Thickness, 80 Icet. Bed C. — Light gray, siliceous grit, sometimes forming a compact, fine- grained sandstone. Seen on both sides of White river. Also at Ash Grove Spring. Thickness, 20 feet. Bed D. — Yellow and light yellow, calcareous marl, with argdlo-cal- careous concretions, and slabs of siliceous limestone, containing well- preserved fresh- ivat'jr shells. On the south side of White river. Seen in its greatest thickness at Pina's Spring. Tliickness, 40 feet. Bed E. — Yellowish and flesh col( .cus ; from Santa Inez mountains, Pecten mrn/nolia, Tapes /.Dezen.sis, Crnssatella cotltna, Mytilus inezensis, Turritella inezann, T. vai'iata, Natica inezfiva. ; from P^strella valley, Cyclas estrellana, Ostrea panzana, Gtycimeris estrellanus, Aatrodapsis anti.selli ; IVom San Buenaventma, 'Tapes muiitana, Periia montana ; from Piijaro river, Santa Cruz, Venns pajaroann ; from the shore of Santa Barbara county, Arcopayia niida; from Sierra Monica, Cyclas permacra, Ostrea subjectc ; Irom San Luis Ol)ispo valley. Area obispoana ; from Salinas river, ^Fonterey county. Dosinia montana, D. snbobliqna ; and from Gaviote Pass, JIactra gavlotensis, and T'rochita costellata. lie described^ from supi)0sed Miocene strata at Rancho Helena, below Salado, Ostrea veleniana, and from Western Texas, in strata supposed to be Eocene, Venus vespertina. I am inclined to believe, however, that this is a Cretaceous species. He described, § from the Eocene of Alabama, Cahiptrophorus trino- diferns. Dr. Thomas Antisell|| made the following section of the Miocene stiata of California, viz : 1. Upper jMioci'ue, consisting of bituminous and foraminiferous beds, tia[)pean coiigionierate, soft, yellow sandstone, foraminiffirous ia;yersand argillite l»cds. Thickness, 400 feet. '•' Expl. and Siir. R. R. Mit-s. Riv. to Pacilic ocean, vo!. vi. ■jr Expl. nnil Siir. U. U. Miff. Hiv. to I'licific oc( an, vol. vii. t U. S. nn'l MfX. Round, Sur. vol. i. g Pro. Aoad. Niit. Sci., vol. ix. Il Expl. and Siir. R. R. Miss. Riv. to Pacific ocean, vol. vii. 184 Tertiary. \ '\ I 2. Middle Miocene, consisting of grits and calcareous sandstones, as at Panza and Santa ^Margarita. Thickness, UOO feet. And the San Antonia sandstones with Dosinia. Thickness, 230 feet. 3. Lower Miocene, consisting of the gvps(;ous and ferruginous sandstones of Santa Inez, Panza, and Gayilaii, containing Osf.rea, and TorrUclhi. Thickness, 1,200 feet. Total thickness of the Miocene, 2,211 feet, but part of this has since been referred to Eocene age. He supposed that the elevation of the Coast Rjmge, in California, above the water level, was an event much later n.' time than tnat of the Sierra Nevada. During the Eocene period, the latter range must have had its crest considerably above water, and was uplifted, finally, after the Pliocene period ; but it is probable that during the whole of ihe 3Ii(ieenc; pe."i';fi, the Coast Range was altogether benea'h the sea level. Anterior to the Post-pliocene period, the erupted rock tilted up their strata, whicli, perhaps, did not reach the level of the ocean sur- face, and upon these smoothed edges, were deposited the unconsoli- daled clays and local drift. They had not, however, fully a[)peared above the surface of the ocean until the close of the Post pliocene period. The elevated sea beaches found distributed over so large an extent of country, from north to south, at a level of from 100 to 150 feet above the sea. and containing species, all of which are now exist- ing, show how comparatively recent is the final elevation of the lower lands of the State, and phices the time of elevation of this range in the earlv portion of the Post-pliocene period. The plutonic rocks of the coast hills, also attest the comparative newness of the land; pumice, obsidian, felspathic lava, trachyte, amygdaloidal greenstone, aulspathic rocks. The soil of the plain is rare!}' quartzose, except when close to some of the low Tertiary hills, which alteration may therefore be due to the wash of these latter. The blue clay is generally assigned by geologists to a slow deposit of mud, proiluced by the sifting action of the tide in estuaries or gulfs where matter is not tran«;portcd by current actions ; it is the evidence of a calm condition of the waters during the period of deposit, and a cessation of upheavals of the land contiguous •, the two beds of bluish clay are separated by nearly forty feet of gravel and sand. The drift gravel (bed 3) consists not only of rounded granitic pe])blcs, but also those of syenite, hornblende schists, metamorphic, brown sandstones, trap and am3'gdaloid ; and the underlying sandy bed is chiefly quartzose, and probably is the detritus of the sandstones at the base of the Cordilleras. There have been no very large stones seen in the drift beds, there are no loose bowlders or erratic blocks, nor is there, either on the sur- face or in the deposits, any stone which can not be traced to masses of similar mineral constitution in the ranges bordering the plain. The period of general or polar drift, therefore, which was one of the earliest of the Post-pliocene epoch, passed by without affecting California ; and it was during the later periods of drift that the processes of wear, ing down cont,inents -and depositing them in the seas around took place, and were carried out on an immense scale, and over an immensely extended period of time. Los Angelos plain is not the only one in California, where these de ■■,!■ I !. 188 Tertiary. |» ft posits of clays and gravels are of great flopth. The borings which have been made in Sacramento and San Joaquin plains have revealed a similar structure of basin, while that in Santa Clara valley, Santa Clara county, shows that the deposit has not been to so great a depth in that plain. Thus, at the Stockton well boring, after passing through red claj's, sands, and gravel, the blue clay was met with at the depth of 400 feet. On the Sacramento valley, between the city and Pit river, the lava clays and sands cover the blue day to the depth ot 358 feet. In the Santa Clara vallej', the covering of clay and light sand above blue clay is from 80 to 115 feet. Blue clays are found 465 feet below the surface at Los Angelos, and, therefore, below the present sea level ; while the surface of the terrace on San Bernardino is somewhat above 2,000 feet in altitude, and as tiie beds are horizontal, or nearly so, it follows that near Los Angelos the deposit took place when the water was over 2,000 feet deep at that point. All the low Tertiary hills were ledges of rock, several hundred feet below low water. The ocean then rolled up east of the Cordilleras, occupying the Colorado desert and the Mohave valley; and the Cor- dilleras stood up like a peninsula in the great mass of waters, with its crests from 3,000 to 5,000 feet above the surface, and with a breadth not more than 60 miles from S. W. to N. E. From the wearing down of the felspathic rocks, the granitic porphyries, and the dark colored shales, arose the blue cla} s, while the trappean and hornblende rocks formed the material of the coarser drift, transported by currents pro duced by the elevations. The carriage of such coarse matter would inevitably remove large portions of the Tertiary hills of the plain, and form the breaks which now occur in what was once a continuous chain, the denuded matter itself going to form the bed of arenaceous clay. It has been calculated that the deposit going on at present in the Gulf of Mexico, produced both by the alluvium of the Mississippi and the transported mud of the Amazon, does not exceed more than half an inch yeai'ly. There is nothing in the topographical condition of Southern California to warrant the belief that the slow deposit could have occurred to a^reater depth in the same space of time; for there is no evidence of the double influence of a large river and a strong current of sea water coinciding. Admitting, however, that the same rate of deposit occurred then as now in the two localities, the period of deposit of the lower blue clay bed would be 7,200 years, and of the upper blue clay and gravels above 1,600 years, making a total of 8,800 years of perfect repose. If to this we add the periods of elevation, both rapid and slow, the total period occupied by the deposit of Post- Mesozoic and Ceenozoic Geology and Pnlmontolouy. 189 pliocene beds, would equal tlie period occupied by some deposits of the Secondary age. Yet such a calculation would scarcely give the total period accurately, since neither has the base of the lower blue clay yet been reached, nor should the present alluvial surface bo looked y\\\ua as the last deposit of that epoch, or the prelude of the modern period; since, the slopes of San Bernardino display a series of conglomerates and gravels 200 feet above the level of the nearest stream (Cajon creek). These are coarse accumulations of primary pebbles and granitic clays, which have been removed from every portion of the plain where it is exposed. In the gorges and canons it still remains ; and wherever a pass has been traveled, there it is found, as the superficial covering, be- tween 200 and 300 feet deep ; this, the last evidence of deposit of the Post-pliocene period, has not been considered in calculation of du- I'ation. Yet such a deposit must have existed over the plain, and must have been removed afterward; so that two additional periods would still require to be added to make the calculation complete, namely, the period occupied by the last deposit, and the period occupied by its re- moval. Prof. J. W. Dawson* said that the mountain of Montreal, in Canada, which rises 700 feet, forms a tide-gauge of the Post-pliocene sea, marking, on its sides by a series of sea cliffs and elevated beaches, the stages of gradual or intermittent elevation of the land as it lose to its present level. The most strongly marked of these sea margins, are at heights of 470, 440, 386, and 220 teet above Lake St. Peter, on the St. Lawrence, or 450, 420, 366, and 200 feet above the river at Montreal. The highest of these beaches contains sea shells of existing species. Below the lowest, and at an elevation of about 100 feet above the river, spreads the grea<: Tertiary plain of Lower Canada, everywhere con- taining marine shells, and presenting a series of deposits partly un- stratified and partly assorted by water. In this vicinity, the regular sequence is as follows : 1. Fine, uniformly grained sand, in some places underlaid or replaced by stratified gravel. Marine shells in the lower part. 2. Unctuous, calcareous claj', of gray, and occasionally of brown and reddish tints. A few marine shells. 3. Compact, bowlder clay, filled with fragments of various rocks, usually, partially rounded, and often scratched and polished. The thickness of these b Is is at least 100 feet, of which the lower or bowlder clay constitutes the greater part, but the sand often attains t\n\ 100 Tertiary. ■ i tho thickness of 10 feot, and tlio fine clny 20 feet. The City of Monticftl is built upon this deposit. The bowlders are not confined to the bowlder clay, but are also found in tlio stratified clays and sand. The bowlders derived from tho mountain, have been drifted to tho southwest, in which direction they have been traced to the south shoreof Lake Ontario, 270 miles distant. The terraces are best seen on the northeast siile of the mountain. The rocks beneath the bowl- der clay, are striated here S. 70° W. and 8. 50° W. In some places the surface of the bowlder clay has been deepl}' cut into furrows by the currents which deposited sand and gravel upon it. In like manner the surface of the stratified clay, is sometimes cut into trenches filled by the overlying sand. All the beds above referred to belong to the close of the Tertiary period, and they are all marine ; but they may have been deposited at distant intervals of time, and in waters of verv various depths and area. From the abundance of the Snxicava rugosa in the upper bed, it was named the Saxicava sand, and from the aoundance of the Leda port- landica, in the middle bed, it was called the Leda clay. Dr. Albert C. Koch* stated that he collected, in 18.39, in Gasconade county, Missouri, about 400 yards from the bank of Bourbense river, where there was a spring, the remains of a Mastodon under such cir- cumstances as to show that it had been burnt to death, and while under- going tliis punishment had also been struck with bowlders and shot with arrows. The animal had evidently been mired as its legs were in an upright position with the toes preserved. The ashes was from 2 to fi inches in thickness, showing that the fire had been kept up for a con- siderable length of time. In the ashes he found stone arrow heads, a stone spear head, and some stone axes. The whole was covered by strata of alluvial deposits consisting of claj', sond and soil from 8 to 9 feet thick. He also stated that about , le year later he found another Mastodon which he called the " Missourium," in Benton county, under about 20 feet of alluvial deposits, and with the bones were several stone arrow heads, one of which la}-^ underneath the thigh bone, and in con- tact with it. * Trans. St. Louis. Acad. Sci., vol. i. Meaoxoir nitil f'trnnzoir Gcohjtji/ tnuJ I^dhionfa/offif. 101 In iN.'iiS, Dr. K. \'. llnyilvn* [)rt'i)!ir('(l a vcitictil section, showing- tlu' order of snpiiposition of tli»^ (Uircrcnt l»(!s fij)p(;ndirtd(tfiin, /'Jcfihioi'iffimnn /xo'viin; tVom near X(!vvbern, Ctir churodoii IfidiKjii/oriit^ Trijiion cdroli'iiciisls; from \Vilmin<;toii, CVo*- chiifodoii cftissidfiis, C. confoi'tidens, ('hhiris mitchdli. Oon/ocfi/iictis Hithamjaldtiia, Lininlifes ohlont/ns; and from other places, Jlemfpn'sfis rreniifftfus. He described, from tlu; Miocene; at Kli>cabethto\vn, and near Cape Fear river, Bladen county. North ('arolina, Polypttichodon riii/osii.K, Ellipfonodun conipressHu, .Fii.sus nqua/is, A', haiiellonns, F, moiiilijoi'- min, Fdsciolaria c/e(/aii.s, F. u/fernnta, F. arnfa, F. nodH/osa, F. apof- rowi, Cnncellaria carolinensis, liuccfntim 7norul(fot')nc, li. mnltiHnent- urn, Vohifa obtusa, Palitdina siibfjlohonti; and from the marl of other places, Gdleocerdo siihcreindits, PijrnoditH cnrolinensfs, Terehra ne- (jlecta, Didium ocfoco.sfjifiim, lUartjuielld con.sfricfii, M. e/erafd, Pleti- rotonid eleijdits^ P. jlexKosiini, P. tuhercuhifum, Pifrmaidelhi reticu- lata, Chemnitzla reticulata, Uu/ima subu/ata, Cerithium annulatum, C. bico.staturn, Terebellum constrictum, ^<;a/aria carta, Litforiaa line- ata, Delphinulv quadricontata, now Carinorbis quadricostatns, Torna' Una cyliiidrictt, Vaicum annu/atuidiiN^ now Pscadivhirus infrcp/'duN, Aelui'odon ferox, Hysfrix t'en- iistii,s\ Castor tortus, C'ervuswui'reni, Menalorneryj' uiobrarensis, 3fery- chyi's ciegatis, M. major, M. medhis, Jlypohippus afffnis, Parahippus coynatns^ Eqitus excelsns, E.fratenius, Protohlppns perditas^ Mery- chippiis mimbilis, lihinoceros crassus, Endephas hnperator, and from tlie red j^rit bed of Niobrara, near Fort Laramie (Miocene), Meryco- choeriis proprius. Ill 18r)0, James Kichardsonf made a geological examination of the r«jisi)e peninsula, and observed two terraces in tho drift to the west of Trois Pistoles river, at loO and 300 feet, resi)ectively, above the sea, and another at the month of the iMa«anne. at the height of 50 feet. Stratifuid clay occurs at the head of lake ^latapedia, 480 feet above the sea and near the outlet at the height of about 530 feet. iNIarine testacoa occur in the terrace on the east side of the Matanne river at the height of 50 feet above the sea; about two miles west of the ^fetis river, at the height of 130 feet, and eight miles up tlie 3Ietis river, at 245 feet above the sea. At the St. Anne river there are five or six terraces in a heiffht of 25 feet, aboundinu' in fragments of marine shells. Grooves and scratches were observed a half mile below Trois Pistoles church, GO feet above the sea, bearing S. 32 deg. E., and on the Kempt road, two miles from Lake Matapedia, G30 feet above the sea, and bearing S. 80 deg. P:. W. E. Logan;); explored the river Rouge, a branch of the Ottawa, to the Iroquois Chute, about fift}' miles from the mouth. He found an nndistnrbed deposit of clay on the left bank of the river, on the fourth i-ange of Grenville, 280 feet above Lake St. Peter, In the rear of Gren- ville and front of Ilanington, not far east of the Rouge, there spreads out a flat surface of several hundred acres in extent, \vh'ch is under- iaid by clay, and has a height of about 500 feet above Lake St. Petei*. The plain of the three mountains has an elevation above the ordinary summer level of the river, of about 30 teet, and above Lake St. Peter of * Proc. Acad. Nat. Sei., vol. x. t Kep. of I'logr. Geo. Sur. of Canada. X Geo. Sur. of Canada, Ifep. of rrojness. Me.sozoic and C(viwzoic Geology and Palo>ontolo ravel at the top, with elay interst rati tied toward the lower part, but the sand greatly predominates. Tlie surface of the rocks in the valley wherever ex- amined were found to be grooved and siriated. The courses of the grooves vary from S. ;J0 deg. E. to S. 25 deg. W., ami accord in a gen- eral way, with the direction of the valley. The limits of the valley evidently guided the direction of the moving masses which prod.uced the striie, Prof. Leo Les(piereux* described, from the Pliocene iieai- Sommer- ville, Fayette countv, Tennessee, Salix densinervin, Qvercus saffordi, Andromeda dnhiii, and JiJUear/nus uKeqi'a/ia'. In 1860, Prof. E. W. Ililgardf divided the Tertiary of Mississippi in ascending order into, 1st, The Northern Lignitic Group; 2d, The Claiborne Group; 3d, The Jackson (iroup; ith, the Vicksbiirg Group; 5th, The Grand Gulf Group. The Northern Lignitic Grouj) occupies the central p:irt of Northern Mississippi, and though generall3' covered by later deposits it out- croi)s at numerous places and is found at ..11 deep borings. It consists of estuary deposits of sandstone, with marine shells; gray clays and sands, and dark brown and yel'ow clays and sands with lignite. Estimated thickness, including the Claiboi iie Group, 425 feet. The Claiborne Group is found in the central part of the northern half of the State, in Holmes, Atahi, Carroll and Choctaw counties, and in the western part of the State in Clarke, Lauderdale, Newton and Scott counties. It consists of blue and white marls, the latter alway-> sandy and often indurate, and sandstones and claystones with some- times lignitic clays an drift materials have passed, and unless these ledges have been decom- posed upon their surfaces, they are covered with scratches or striie, usually parallel to one another, and indicating the course of the drift agency. Ledges of talcose and argillaceous rocks preserve these mark- ings the most distincth'. Were the rocks of Maine laid bare, fully half the surface would show these marks of smoothing. The course of the strijie in Maine vary from north 70 dog. west to north 80 deg. east. At the Lubec lead mines, a series of striie were observed upon the side of a perpendicular wall, foUovving the course of the wall around a corner. The course of the strioe ultimately varied at right angles from their original directions. At several places at the sea shore the stria; have been noticed below high water mark, and others were seen to run under the ocean at low-water mark. The course of the strife upon the lakes north of the Katahdin mountains have more of an easterly course than those to the east and south of the same mountains. It looks as if the mountains formed an obstruction around which the striating agency operated, in preference to climbing the elevation. It is a curious fact, in the same connection, that. the strire are wanting on the sum- mit of Katahdin. It ajjpears also that there was another deflection of the course of the strisx; in the valley of Sandy river. Mt. Abraham may have arrested the drift current on the north and iiirned it into Sandy river valley on the west, from which deflection it struck against the Saddleback mountain range, continued to Mount Blue, and was then directed toward French's Mountain in Farmington. Drift strije are never found upon the south side of mountains, unless for a short distance, where the slope is very small. It is common to see different courses of stria? intersecting one another, as on the south side of Chamberlin lake, where strisB north 70 deg. west and north 50 deg. west intersect, and north 17 deg. west and north (>7 deg. west in- tersect. The only examples of glacial markings discovered, in Maine, are on the St. .lohn river, in its upi)er portion. Above the Lake of the Seven Islands, on this rivei', there are no glacial markings, unless the scratches upon the pavement of bowlders .ire to be referred to them. The bed of the river is full of stones, and upon the banks below high- water mark they are as (irmly set as paving stones in the streets of a city. The scratches are not as constant and distinct as those of the glacier below, and may pos; ibly have been formed by ice freshets in Mcsozoir. and Caenozoic GeoJopi/ find PidmontoJag^i. ion high , of a of the lets iu the spring of the yojir. Dcsf-cMidiuu the river to No. 14 we lind a, h'dge whieh has been stniek h\ a foree (leseeuding the river, as tiiestoss and lee sides plainly show. The coarse of the striiB is north 0.') deg. west, the stoss side heing on tlie southeast. A similar example occurs neai' the juoiith of Hlack rivei', where tiie course of the stria; is toward noith 8 bclli/ii'dfus; from VicUsbmu', 'relliua nnryfernui ; from ;i brown, highly ferruginous s!in(lstonoiitC:i(l(lo Teiik, Texas, Mcretrix yoakiuin\ Perna tcxdna ; from Houston county. Toxas, Profocardin (/(tmbrinn : and from Soutli Carolina, Oslrca niorf'mi. He doscrilxMl, fi'om tlie Mioeene of \'irginia, VoUita sinnosn; from Santa l?arbara, California, Tnrhonilhi tis/xira, now BltHinr. (isperinn. Modi'Jin sf.i'/fif(i, Uoi'dhti'ln niif).iiii((, Spheiiid bil/Vfit", Venus rhj/tionu'n, Cardifjt inoH/lirosta, and MoiTisia /lonii. Prof. Leo. Losquereuxf des(!ril)e(l, from the Pliocene beds at Brandon, Vei'mont, (UirpoliHies brandotiniins, (', hrfnidonanus, vav. elonijahis, ('. hrandonanus, var. obtvsiis, ('. Jiss/'lis, C. tire y (inns. C. irregnlaris, Cdvyn nennonfjina, C. verrntujsa, FiKjns liiti'.hcocki,. Apeibopnis f/au- dfni, A. heeri, ArustoJocftia cnrvafu, A . ohscnrn, A. (imint/cn.sis, Supin- dns funcficrninfi, Ciirpolithes bnrsdcforniLs, Cinnanwinnni novaidnyUa', Illicium liijnif.nm, Drnpa rhnbdosperma, jYi/sun compldnatfi, iV. lorviy- ata, and J^. microciirpa. In 18H2, Gal)b and Horn); described, from the Eocene, near Charles- ton, South Carolina, Est-hara fcxtc, Itepfescliarelld cdrolinensis ; from Claiborne. Alabama, Enchard ovalis, Seniieschdra fnbnldfd, Cellcpora cycloi'is, ('. hiorndfd, J'Jftchdrelld inicropord : from Vicksl)urg, Missis sippi, lieptocel/epovd rid yhnueratd. They described, from the Miocene of St. JMary's riv(>r, Maryland, Eschdva frdy ilisshiKt ; from Petersburg, Va., Enndlipord qnadranyu- lan's; from the ^liocenr, of New Jersey, deUepora iirceo/dtd, Mem- branip(}ra se.vpinictdfM, llept.ojiustrelld tnbidata : from Santa Barbara, California, Seinitubiyei'd tnba, E)itdlophor(t punctnlafd, Ce/lepora cdliforriensis, C. belleropl/on, lieptesahdrelld Iieernidiini, P. pUind, Phklolopoi'd Idbiatd, Peptoporina en.sfonidta, Repteschdrellina dis- pnrilis^U. heermdnni, P. covnfitd, Siphonelhi vmlflpord, Jfcmbrdnipora calif ornicn, Vrisind serratd^ and Lirhenopord cdli.fornird. T. A. Conrad§ described, from the Miocene of Virginia, Surcula enyoudtd, S. nodnliferd, Drillia impretisd, D. distdns, D. aratd, D. be/la, D. eburned, Jldiiye/id viryiniana, Pleiorytis ovdto., Pnsycon curi- ndtinti, B. Jflosnni, l^riNd scdhiris, now Bncrinnm scaldre, Astyris re- ticulata, Dactylus eburens, now Oliva eborea, Leiotrochus distans, * I'rih-. .\c;i(l. Nut. Sci., vol. xii . -f Gcol W'l'inoiit, vol. ii. t Jour. Acad. Nat. Sci., i<\ .ser., vol. v. •^ Prof. Acad. Nat. Sci., vol. xiii. Menozoi'c and dcnuozot'c Geohxji) and Pahvonfolixji/. 203 I'ecteii J)'(i/cj')iiis, liitsycon fi'i/oiu's, MeUimpnx /onr/idciis, .}f)icfri>hi>r(i nthh-Jn, DiohC densafd, ;iii(l D. I'hujiniiina ; IVoin Calvort dills, iuid St. Mary's comity. Mary- hiiul, Siirriihi ri((/af.fi, IhtUiopsix mnnjhnidicn, B. tH-afd, .Ishjris '(tin- mvnin, A. (ivara, var. f/rdnii/f/erd, and JJimijcoii (t/vciifinii : IVoni South Caroiina. A nonifilocfirdia tn'tiintinarifi ; tVoni North (.'aroliiia, Den- tiilhnii c((ro/inciisc, Pccten edifccomettsis^ Xoe.thi tuo'oJinensis, Ducfi/l- i(s caroliiiens/'f), now 01 Ira lutvolinensis, and SiHqnurla cdrolineiisis; tVoin Ciiinborland t'ounty, New Jersey, Tiiri'ifclhi (vqiilstriafa, T. cinii- herhiiidld. SdxicdVd, vii/d'formis, f'drdifamerd dfn/nafd, aiul Astdvtc (listdiis-; from California, Lyropecfen crass tea rdo ; and from tlio Koi-eno, at P^ntcrprisc, Clark county, ^Ilssissippi, Crds-sdfelhi proOncta. Wm. Stimpson described, IVom the I'ost-plioeene at CapoIIoix', on the southeast side of Hudson's T)ay. lUu'dinm dcirsoiu'. Along Lake Temiseamang, * t'he Ottawa river and Riviere Houge. north of the Ottawa, the furrows conform in a gvneral way to tiie di- rections of the river- valleys, the limits of which appear to have guided the moving masses which produced the grooves. Tlu; direction of the grooves at a single locality is not onl\' not uniform, but, on the contrary, they frequently cross each other. ^Measurements taken at 145 differ- ent places in Canada show that there is no uniformity in the directtion of the striic, but as in these cases they vary from S. 80° E. to S. 70° W. Bowlders are found in great abundiince in nuiny places, especially in the valleys, wiiere the bowlder formation has been extensively denuded by the action of the water, and its lighter materials swept away. On elevations, they are often seen resting upon the unstratilied drift, Avhicli, in the adjacent depressions of the surface, is covered over by strati- lied sand and clay. They appear, in most instances, to have traveled southward, V)ut there are exceptions to this general rule. Thus in the county of Rimonski, in the valley of the Neigette river, there are lai'ge bowlders of limestone, one of them 40 feet in diameter, belonging to the Gaspe series, which have been moved several miles northward or north- eastward. Farther down the valley of the St. Lawrence, l)!ocks of trachytic granite have been carried northeastward from the Table- topped mountain down the valley of the ^Ligdalen. There arc; also instances of the northward trans[)ortaftion of bowlders in Nova Scotia. The valleys of the St. Lawrence and the Richelieu, in Canada East, and a considerable portion of tin; region between the St. Lawrence and T'!|- ( * Geo. ofCauada, 1803, 204 Ternary. .. t-, llic Ottiiw.'t, to the cnst of the iiicridiun of Kiii,i>stoii, aro occupied li\ sU'Mtilicd clays, wliicli, iinliUi^ those of western Caiiathi, contain alxindatice oi' marine shells, lor tin; most |)art identical with species now livinji' in the lower St. Lawrence and the yiiH'. The clays are in many cases overlaid by sands, occasionally interstratilicd with clay, which also contain marine remains. The two are reyardefl as (orminy parts of one formation, and as coi'res|)ondin<^" to the upper and lower divisions of the (Jhamplain clay o N'ermont. The lower divi.sicni is calleil the Fjcila clay, and the upper the Saxicava saml. If a line he drawn IVom the onllet of Lake (Miamplain to Ottawa, and from the extremities of this, as a l)asc, two others he carried to (^nehec, there will I)C! incliule(l a very level triangular area of aI)ont 9,000 square miles, for the greater part covered by the Champlaiii clays and sands. The plains on either side of the St. Lawrence lielow Quebec are occu pied by the same formation, which is found at intervals as far down as 3Iatanne; while on the north side it covers an extensive area in the valley of the Saguenay and around lake St. .John and its tribu taries. Clays belonging to the lower division are found at various levels from the surface of the sea to GOO leot above it, and in some cases they have been observed some feet below the sea-level. The rivei- U()Ug(^ enters the Ottawa between hills of bare rock; l)ut on its >vestern side, in the fourth range of Grenville. a bank of clay 1:^5 feet in thickness occurs, the summit of which is 405 ieet above the sea. Again, not far east of tills river, in the rear of Grenville, and in the front of Harrington, is an tirea of sevei'al hundred acres, underlaid by .stratilied blue clay, the surface of which is about ')00 feet above the sea. Several similiar portions of clay occur in that vicinity. In Gaspe, at llu! head of Lake 3Iata|)edia, stratilied clay occurs at the height of 480 feet, and near the outlet of the same lake, at the height of 5.30 feet above the sea. At Bay St. I'aul, oa the north side of the St. M Lawrence, terraces occur at lIJO and 360 feet above the sea. lAIarine fossils occur throughout the strata in which those terraces are worn, and still highei" at IJOO feist above the sea level. In the valley of the Saguenay, marine cla_ys, generally overlaid by sand and gravel, are I'ound almost everywhere between Ila-ha bay and the west side of Lake St. Johns; as well as between that bay and Chicontimi. Between Chi- contimi and Ha-ha bay the clay is sometimes GOO feet in thickness. About a half mile below the falls of Bell Riviere, marine shells occur in the clay at 400 feet abov(! the sea. The Saxicava sand forms a belt on the north side of the St. Mesozoir (t)nl Cnnnzoic Geolnijn mid I'uhvontahtijy, 205 Liiwrcnco, at the basi? of tlic Tiiiiirciitidc liills, fniin Ottjiwii t(» C'apf 'I'oiirinciilc. It, »'X|)!111(Ih on the Si,. Miiiiricc lo a iMctiiltli of tliiitv milcH. To llu' westward it covt'cs imicli ol llu' siirfari! in tlu' Iriaiimi hir area hotwccii tiu! St. Lawrt'iico and tlu^ Otta^va oast oftlir meridian of Kingston. .Marine slieils oceiir in this .s.-iiid in N»'|»e:in, at 410 feet above tli(f sea ; in Keiiyon, at "iWh feet ; in FitzroVi "*^ •»'^'* '"^'^'^ 1 '" Wineiiester, at iJOO feet , and at raUenliani nulls, :it 22() f«'et. South of the St. liawrenec! these sands aii' found aloni; the Ixtnnd.-iry of New Voi'k. From tii(( cast side of .Missiscinoi l)ay, a i)elt extends between the clay plains of th(> sonth sliore of the St. I/iwrenee, wliieli it partly overlies, and the more elevated region to the sontheast, as far as Metis. At the Wiillhriduc ."Mills, in Stanhridi^'e, marine .shells oeeur at a height of 1(50 feet, and near Upton, on the (ir;ind Trnnk railway, at l{()0 feet above sea level. In 18();{, J. S. Newberry ■ described, from the Miocene of r»el!in<;hain bay, Eqiilsetnm rolmsfmn, Sabal cjimphcJ/f, Querent corioecu, Q. Jfexuona, Q. h((iilcsi in tin iiioiinfaiii.s, iiiul Unit llicy Ik'Ioiih lo tlu' Mirtcciic 'l^'i'ti;ir\ . At .-iImhiI six iiiilcs iVdiii Sruitii ( 'ni/, aio suiiic siiiiiiihir «'\aiii|)li's of \V( atlicn i| MaiKlstuiic, wliifli arc known as the '• Kiiiiis "' or the •■ IJniiioil Citv." II oro |)or|i 'iiilicnlar I iilics or i-liiiiiiu'V's ol' rock .'ir(> round, rioiiioiit'li tliroc It'i'l. ill diamolor, the sainlstKiio a|)|)oarinn' to Ii;ivt' hi'on liaiiliiicil ill concent ric layers liy liic inllltratioii ol" rcirii'^iiioiis solutions, ;in0 to liOO foot thick, rostinu nncon forinal)ly upon altorod strata. The rocks luw soft, yellow sandstone. witli laryo nodules of iiard. hliio calcareous sandstone, imix'dded in them. Hotweon the hii;host |)t)ints near the lioad of Tomales hay and Piinta Keyes, thoro are minor riduos of .Mio(;ono sandstone, havini!, a low southwest dip. The sandstoiu!s of the Santa .^[onica and Snnta Susanna Ranges, are, in largo part, of Mioci.'iio age. The ridgos hounding tlio San Fernando valley on the southwest, are made up of light bituminous slates, dipping generally to the east or north east : they form roundeil hills, bearing the marks of extensive erosion. A higher range to the west of these hills eonnoots the two chains, and rises to a height of ;5,000 feet above the sea, being made up of Mioei'iie sandstones, highly inclined and in some plaees metamorphosed. The eluiin of the Santa Inez Range rises to the north of Santa IJar- bara. a conspieuous oltjeet to those a[)proaehiug this place by water. As far as known, it takes its origin at a point S. linlca, (Jochlespirti enyonata, Moniliopsiti elaborafa, Drillin texana, Tortolira texana, Monoptyyma curta, Volutilithes indenta, V. impressa., Obeliscns perexilis, Architectonica '. i ■'•' Pro. Cal. Aciul. Sci. V Pro. Acad. Nat. Sci. I Am. .Tour. Coiicli., vol. i. '^ Am. Jour. Couch., vol. i. rrp^ 210 Tertiary. ' < coelatura, Gancellaria impressa, C. tortiplicn, Tornatellaui l(ita,Corhula fllosa, JUgeria donneaa, Cytheriopsis hydnno, Cyclas claihornensis, Mysia deUoidea, Conns alveafiis, C. siibsauri'dens, CocMeapira bella, Htccciirif.on altum, Limatia marylcotdica, ClrsoHtreiaa claibornensis. Gancellaria ellapsa, Dentalium densatinn ; from Shark river, Mon- mouth count}', New Jersey, Pleurotomaria perlafa^ Snrcula annosa, Actaionema prisca, and Avicula annosa. In 186(1, Prof. J. W. Dawson* said the snow-clad hills of Green- land send down to the sea great glaciers, which in the bays and fiords of that inhospitable region, form, at their extremities, huge cliffs of ever- lasting ice, and annually " calve," as the seamen say, or give off a gi'eat progeny of ice islands, which slowl}' drifted to the southward by the Arctic current, pass along the American coast, diffusing a cold and bleak atmosphere, until they melt in the warm waters of the Gulf stream. INIanj^ of these bergs enter the straits of Belle-Isle, for the Arctic current clings closely to the coast, and a part of it seems to be deflected into the Gulf of St. Lawrence through this passage, carrying with it manj' large bergs. Mr. Vaughan, late superintendent of the light house at Belle-Isle, has kept a register of icebergs for several years. He states that for ten which enter the straits, fifty drift to the southward, and that most of those which enter pass inward on the north side of the island, drift toward the western end of the straits and then pass out on the south of the island, so that the straits seem to be merely a sort of eddy in the course of the bergs. The number in the straits varies much in different seasons of the j'ear. The greatest number are seen in spring, especially in May and June; and toward autumn and in the winter very few remain. Tliose whicrh remain until autumn are reduced to mere skeletons; but if they survive until winter, they again grow in dimensions, owing to tlie accumulations upon them of snow and new ice. Those that we saw early in July were large and massive in their proportions. The few that remained when we returned in September, were smaller in size, and cut into fantastic and toppling pinnacles. Vaughan records that on the 30th of Maj^ 1858, he counted in the straits of Belle-Isle 490 bergs, the least of them 60 feet in height, some of them half a mile long and 200 feet high. Only ,^ of the vol- ume of floating ice appears above water, and man}' of these great bergs may thus touch the ground in a depth of 30 fathoms or more, so that if we imagine 400 of them moving up and down under the influence of * Can. Nat. & (ieol., 2d series, vol. iii- Mesozoic and Cmnozoic Geology and Palceontology. 211 the current, oscillating slowly with the motion of the sea, and grind- ing on the rocks and stone-covered bottom, at all depths, from the cen- ter of the channel, we may form some conception of the effects of these huge polishers of the sea floor. Of the bergs which pass outside of the straits, many ground on the banks off Belle Isle. Vaughan has seen a hundred large bergs aground at one time on the banks, and they ground on various parts of the banks of Newfoundland, and all along the coast of that island. As they are borne by the deep seated cold current, and are scarcely at all affected by the wind, they move somewhat uniformly, in a direction from N. E. to S. W., and when they touch the bottom the striation or grooving which they produce must be in that direction. In passing through the straits in Jul}', we saw a great number of bergs, some were low and flat topped with perpendicular sides, others were conca.e or roof-shaped like great tents pitched on the sea ; others were rounded in outline or rose into towers and pinnacles. Most of them were of a pure dead white, like loaf sugar, shaded with pale bluish green in the great rents and recent fractures. One of them seemed as if it had grounded and then- overturned, presenting a flat and scored surface covered with sand and earthy matter. After describing the glaciers of Mont Blanc, he lays down the following rules : 1. Glaciers heap up their debris in abrupt ridges. Floating ice sometimes does this, but more usually spreads its load in a more or less uniform sheet. 2. The material of moraines is all local, icebergs carry their de- posits often to great distances from their sources. 3. The stones carried by glaciers are mostly angular, except where the}' have been acted on by torrents. Those moved by floating ice are more often rounded, being acted on by ulie waves and by the abrading action of sand drifted by currents. 4. In the marine glacial deposits, mud is mixed with stones and bowlders. In the case of land glaciers, most of this mud is carried oft' by streams, and deposited elsewhere. 5. The deposits from floating ice may contain marine shells. Those of glaciers can not, except where, as in Greenland and Spitzbergen, glaciers push their moraines out into the sea. 6. It is the nature of glaciers to flow in the deepest ravines they can find, and such ravines drain the ice of extensive areas of mountain land. Icebergs, on the contrary, act with greatest ease on flat sur- faces, or slight elevations in the seat bottom. TT^"" 212 Tertiary, :fs ' 7. Glaciers must descend slopes, jind must be bucked by large sup plies of perennial snow. Icebergs act independently, and being water- borne, may work up slopes and on level surfaces. 8. Glaciers striate the sides and bottoms of their ravines very un equally, acting with great force and effect only on those places wheii" their weight impinges most heavily. Icebergs, on the conti-ary, beinu carried by constant currents, and over comparatively Hat surface-'. must striate and grind more regularly over large areas, and with less reference to local inequalities of surface. 9. The direction of the striai and grooves produced by glaciers de pends on the direction of the valleys. Tliat of icebergs, on Ihe con trary, depends upon the direction of marine currents, which is not determined by the outline of surface, but is influenced by the large and wide depressions of the sea bottom, 10. When subsidence of the land is in progress, floating ice may carry bowldere from lower to higher levels. Glaciers can not do this under any circumstances, though in their progress the^^ may leave blocks perched on the tops of peaks and ridges. He further said, that, in all these points of difference, the bowlder clay and drift of Canada, and other parts of North America, cor- respond rather with the action of floating ice than of land ice. More especiall}' is this the case in the character of the striated sur faces, the bedded distribution of the deposits, the transport of mate- rial up the natuial slope, the presence of marine shells, and the mechanical and chemical character of the bowlder clay. He als ) enumerated the following Post-pliocene plants as occur ring, in nodules, at Green's Creek, and other places in Canada to wit: Drosero, rutundifoU'.t, Acer spicatum, Potentilla canadensis, Gai/lxs- saccia. resinosa, Populas balsainifera, Thuja occf.denlalis, Potaino- (/et'm perfoliatas, P. pusillus, Equisetam scirpoides. None of the plants are properly Arctic in their distribution, and the assemblage may be characterized as a selection from the present Canadian flora of some of the more hardy species iiaving the most northern range. At Green's Creek (near Ottawa) the plant-bearing nodules occur in the lower part of the Leda clay, which contains a few bowlders, and i.s apparentl}', in places, overlaid by large bowlders, while no distinct bowlder clay underlies it. The circunastances which accumulated the thick bed ot bowlder clay near Montreal, were probably absent in the Ottawa valley. In any case, W(; must regard the deposits of Green's Creek as coeval with the Leda clay of Montreal, and with the period Mesozoic and Ccenozoie Geology and Palceontology. 213 of the greatest abiii. ar/e of Leda truncata, tlie most exclusively Arctic shell of these deposits. In other words, he regarded the plants above mentioned as probably belonging to the period of greatest re- frigeration of which we have any evidence — of course, not including that mythical period of universal incasement in ice, of which, in so far as Canada is concerned, there is no evidence whatever. The Tertiary formation * exists in the sontliern part of the State of Illinois. It is best developed in Pulaski and Massac counties. It is represented by a series of stratified sands and clays of various colors, with beds of silicious gravel, often cemented into a ferrugin- ous conglomerate by the infiltration of a hydroxyd of iron. In some places it contains green, marly sand, with casts of fossils, and along the edge of the Ohio, at extreme low water, at Caledonia, there is a thin bed of lignit(!. At Fort Massac, just above Metropolis, the fer- ruginous conglomerate is from forty to fifty feet in thickness. Near Caledonia, a section gave a thickness of 56^- feet. T. A. Conradf described, from the Miocene of the Eastern and Southern States, Nassa suhcylindrica, Volutifnsus typtis^ Cancellarki ficalarfna, Saxicavn paril/s, Spisula capillar) a, Tellinn peraeuta, T. capillifera, Astarte com.psonema, Lithophaga si/halveata, 3facomn rirginiava, Mercennria obfusa, and Cnmingia medinlis. Philip P. Carpent .•;); described, from the Pliocene of Santa Barbara, California, Turrifella, jeweffA, Bittium armillatitm, Opalin insculpta, Trophon fennisGidpfus, and Pisaniafortis. In 1867, Prof. Vj. W. HilgardjJ said that nowhere has the geologist more need of divesting himself of reliance upon lithological characters, than in the study of the Mississippi Eocene. Not only do the m.iteri.als of the different groups often bear a most extraordinary resemblance to each otiier, but their character varies incessantly, in one and the same stratum, within short distances. Hale remarks that in Mississippi, the Orbitoides limestone seems to be represented by blue marlstone, and so it is, sometimes. But while on the one hand we see the hard limestone of the Vicksburg bluff passing into blue marl (Byram, Marshall's quarry), we on the other hand find it passing equally Into a rock undistinguishable from that of St. Stephens (Brandon, Wayne county) ; the varied fossils described by Conrad disappearing almost •'•' Geo. Sur of Til., vol. i. t Am. Jour. Conch., vol. ii. i Ann. k Mafr. Nat. Hist., 3d sor., vol. xvii. 'J Am. Jour. Sci. & Arts, 2(1 ser., vol. xliii. 214 Tertiary, '1 entirely, to be replaced by millions of Orbitoides imbedded in a semi indurate mass of carbonate of lime, interspersed at times witli similar- ly constituted conglomeratic masses of Pecten pouhoni. He could not, therefore, agree to the propriety of distinguishing as separate divisions the Orbitoides limestone, and the Vicksburg Group, The oceurrenceof a different species of Orbitoides (0. Dvpera) at Vicksburg, does not alter the case, for the undoubted O. mantelfi occurs there also, in the solid rock. And there are few of the chanicteristic fossils ol" the Vicksburg profile, which do not, on some occasi/)ns, occur side by side with the O. manfelh', and its com])anions, Pecten pouhoni and Ontrea vir.kshvrgensis. Of course, the coral '>ad its favorite haunts — the moUusks theirs. There is nothing surprising in the fact, that where one abounds, the others are usually scarce, or vice versa. He regarded the Shell Bluff Group of Conrad, or the Red Bluff Group — No. 4 of the Vicksburg section — which is charactei'ized by the occur- rence of Ostrea f/eorginna, as more or less co-extensive with the Vicks- burg Group, and regularly associated with it, as a subordinate feature. Its inconsiderable thickness readily explains its entire absence at many points, where, stratigraphically, it ought to appear. Prof. E, D. Cope* described, from the Miocene of Charles county, Maryland, Eschrichfius cephalus, Jihahdosteiifi lafiradix, Squalodon menfo, Aetohatis profundus, Myliohatis (jigfts^ M. pacJif/odon, M. vi- comicanus, Raja dux\ ^otidanus plectrodon, Galeocerdo loivisshnus, Spfiyrna magna, Trionyx cellulosus, Thecachampsa contusor, T. seri- codon, Orycterocetus crocodflinus, Priscodelphinvs acutidcns, Esch richtius lepfocentrus, Squalodon protervus, and Galcra macrodon. T. A. Conradf described, from the Eocene of Texas, Venericardia mooreana; from the Miocene of the Eastern and Southern States, Plev- romeris decemcostata, Mactra contractu, M. virginiana, Lucina den- sata, Cardium emmonsi, 3Iercenaria percrassa, 3fnlinia par ills, Semete caroUnensis, Abra rmculiformis, Corhula curti, Pecten tricar i- nntus, P. yorkensis, Sycotypus pyriformis, Cylichna, virginica, Zizy- phinus briani, Z. punctatus, Neverita densnta, K. emmonsi, Ptiicho- salpinx, scalaspira, Paranassa granifera. Bursa cenfrosa, and Bnsy- con dumosum. Prof. Gill described, from North Carolina, Sycotypus clongntus. In 1868, Prof. J. W. Dawson;J; offered the following reasons, to show, * Proc. Acad. Nat. Sci. t Am. Jour. Conch., vol. iii. I Acadian GqoloKy. Mesozoic and Ccenozoio Geology and Palaeontology. 215 show, that the drift deposits of eastern America are not to be accounted for upon the theory of a terrestrial origin or a supimsed glacial period. 1. It requires a series of suppositions unlikely in themselves, and not warranted by facts. The most important of these is the coincidence of a wide spread continent, and a universal covering of ice in a temperate latitude. In the existing state of the world, it is well known that the ordinary conditions required by glaciers in temperate latitudes are elevattid chains and peaks extending above the snow-line; and that cases, in which, in such hititudes, glaciers extend nearly to the sea level, occur only where the mean temperature is reduced by cold ocean currents approaching to high land, as for instance, in Terra del Fuego, and the southern extremity of South America. But the temper.'ite re- gions of North America could not be covered with a permanent mantle of ice under the existing conditions of solar radiation; for, even if the whole were elevated into a table-land, its breadth would secure a suf- ficient summer heat to melt away tiie ice, except from high mountain peaks. Either, then, there must have been immense mountain-chains which have disappeared, or there must have been some unexampled as- tronomical cause of refrigeration, as, for example, the earth passing into a colder portion of space, or the amount of solar heat being dim- inished. But the former supposition has no warrant from geology, and astronomy affords no evidence for the latter view, which, beside, would imply a diminution of evaporation, militating as much against the glacier theor^^ as would an excess of heat. An attempt has recently been made by Professor Frankland to account for such a state of things, by the supposition of a higher temperature of tlie sea, along with a colder teuperaturc of the laud; but this inversion of the usual state of things is unwarranted b}^ the doctrine of secular cooling of the earth; it is contradicted by the fossils of the period, which show that the seas were colder than at present; and if it existed, it could not produce the effects required, unless a preter-natural arrest were at the same time laid on the winds, which spread the temperature of the sea over the land. The alleged facts observed in Norway, and stated to support this view, are evidently nothing but the results ordinarily observed in ranges of hills, one side of which fronts cold sea-water, and the other land warmed in summer by the sun. The ..ipposed effects of the varyirg eccentricity of the earth's orbit, so ably expounded by Mr. Croll, are no doubt deserving of considera- tion in this connection; but I agree with Sir Charles Lyell in regard- ing them as insuflicient to produce any effect so great as that refrigera- Tf^ It 216 Tertiary. tlon suppoHed by the theory now before us, even if aided b}' what Sir Cliarles truly regards as a more important cause of cold — namely, a different distribution of land and water, in such a manner as to give a great excess of land in high latitudes, 2. It seems physically impossible that a sheet of ice, such as that supposed, could move over an uneven surface, striating it in directions uniform over vast area., and often different from the present inclina- tions of the surface. Glacier ice may move on very slight slopes, but it must follow these ; and the only result of the immense accumulation of ice supposed, would be to prevent motion altogether by tlie want of slope or the counter-action of opposing slopes, or to induce a slight and irregular motion toward the margins, or outward from the more prominent protuberances. It is to be observed, also, that, as Hopkins has shown, it is only the sliding motion of glaciers that can polish or erode surfaces, and that any internal chan<'es, resulting from the mere weight of a thick mass of ice resting on a level surface, could have little or no influence in this way. 3. The tiansport of bowlders to great distances, and tho lodgment of them on hilltops, couhl not have b(!en occasioned by glaciers. Tliese carry downward the blocks that fall on them from wasting cliffs. But the universal glacier supposed could have no such cliffs from which to collect ; arici it must have carried bowlders for hundreds of miles, and left them on points as high as those they were taken from. On the Montreal Mountain, at a height of 600 feet above the sea, are huge bowlders of feldspar from the Laurentide Hills, which must have been carried oO to 100 miles from points of scarcely greater elevation, and over a valley in which the strifxi are in a direction nearly at right angles with that of the probable ('riftage of the bowlders. Quite as striking examples occur in many parts of the countr}'. It is also to be observed that bowlders, often of large size, occur scattered through the marine stratified clays and sands containing sea-shells ; and what- ever views may be entertained as to other bowlders, it can not be denied that these have been borne by floating ice. Nor is it true, as has been often allirmed, that the bowlder clay is destitute of marine fossils. At Isle Verte, Riviere du Loup. Murray Bay, and St. Nicholas on the St. Lawrence, and also at Cape Elizabeth, near Port- land, there arc tough stony clays of the nature of true " till,'' and in the loiver part of tho drift, which contain numerous marine shells of the usual Post-pliocene species. Mesozoic (Did Ca'tiozoic Geoloyy aii upper both tic current would ding to the Northern jjind, or l)e tlirown mo rapidly to the west that its direct action niij^ht not reacli sucii summits. Nor would I exclude alto;^ether the action of glaciers in eastern America, though I must dissent from any view which would assign to them the principal agenc}' in our glacial phenomena. Under a condi- tion of the continent in whi(!h only its higher peaks were above tlie water, the air wou^l be so moist, and the temperature so low, thati)er- manent ice may have clung about mountains in the temperate latitudes. The striation itself shows that there must have been extensive glaciers, as now, in the extreme Arctic regions. Yet I think, that most of the alleged instances must be founded on error, and that old sea-beaches have been mistaken for moraines. I have failed to find even in our higher mountains any distinct sign of glacier action, though the action of the ocean breakers is visible almost to their summits; and though I have observed in Canada and Nova Scotia many old sea-beaches, gravel-ridges, and lake-margins, I have seen notiiing that could fairly be regarded as the work of glaciers. Tiie so-called moraines, in so far as m\- observation extends, are more probably shingle beaches and bars, old coast-lines loaded with bowldei's, trains of bowlders or " ozars." Most of them convev to mv mind the impression of ice-action along; a, slowly subsiding coast, forming successive deposits of stones in the shal- low water, and burning them in clay and smaller stones as the depth increased. These deposits were again modified during emergence, when the old ridges were sometimes bared b}' denudation, and new ones heaped up. We now have, in all, exclusive of doubtful forms, about one hundred species of marine invertebrates, from the Post-pliocene clan's of the St. Lawrence valley. All, except four or five species, belonging to the older or deep water part of the deposit, are known as living shells of the Arctic or boreal regions of the Atlantic. About half of the species are fossil in the Post-pliocene of Great Britain. The great majority are now living in the Gulf of St. Lawrence, and on the neighboring coasts; and more especially on the north side of the gulf and the coast of Labrador. In so far, then, as marine life is concerned, the modern period in this country- is connected with that of the bowlder clay by an unbroken chain of animal existence. These deposits in Lower Canada afford no indications of the terrestrial fauna ; but the emains of jEleph((s primigenius, in beds of similar age in Upi)er Canada, show that during the period in question, great changes occurred among the animals of the land ; and we may hope to find similar evidences else .!*3 TW I 220 Tertiary. whoro, ospncinlly in looalitios whoro, as on i\\v. Ottawa, tho debris of land-pIantH and Itnid-Hlu'lls iwvwv in tho injirinc dcpositH. Tho EotHMio of Now JiTscy* in laiown as \\u\ Tppcr marl Itccl, juul has a thickness (»f ;}7 foct. Fossils arc al)un(hint wherever iniirl pits have boon opened, l)etvvt'en Deal on tlio sea shore and Clementon in Camden connty. Tlu! IMiocenc is recognized by its fossils in man^' locjilitios in New Jersey. It is not always c()n(V)rmal)l(! witli the pjocene below, and its thickness is variable. In 180S, rrof. E. D. Copef described the Miocene deposit of the western shore of Maryland, as coiisisliiiij of a dark, sandy clay, vary- ing from a leaden to a blackish color, throngh which water does not penetrate. Its npper horizon intiy be traced along the high shores and cliffs of the Chesapeake by the line of trickling nprings which follow its upper surface. A great bed of shells occurs at from fourteen to twenty-two feet below its upper horizon. He described, defophis helcroch'tus, Txcwanthiis (uvloHitondjiJns, Pris- codelphinits .spitiosifs, now Bclosphijs .spitio.sns. P. nfro/n/'s, now /?. atropiiis, P. stetms, now Ji. sfenus, ZarharJii's Jlanelhifor, Delphin- npterns raschenheriicri, now Trefosplnjs ruschenberf/eri, D. lacerfosns, now T. hu'.ertosus, D. f/nbbi\ now T.gdbbi, 7). h(iwki»si\ now 2\ haivkinsi, D. tyrnnnus, now Eschrictiiis fi/ranni's, JJ. pusillus, Jref/nptera e:i'pa)isa, now E. expnusus; from the P^ocene green sand of^Ioumouth county. New Jersey, Pidivophis ha/idaiiKs, and P. littoralh. Isaac Lea described, from a Miocene deposit, six miles northeast of Camden, New Jerse}', ?/»/o ala/oides, U. carn'osoi'dcs, U. Immerosoi- de.s; U. nasntokles, U.radiatoidcs, U. subroti'iidoides, U.roanokoiden, U. ligavientuwides, U. f/randioides, and U. corpulentoldes. Dr. Joseph Lcidy described, from blue clay and sand beneath a bed of bitumen of Pliocene age, in Hardin connty, Texas, 3Ief/(donjjx vnh- dus^ Tni('(felisfaf alt's, and Emys petrolei; from "Douglas Fhit, Calav- eras count}', California, Elotherium avpcrbioti; from Martinez, Equns puciflcHs, the largest known fossil horse tooth: from Ashley river. South Carolina, Iloplocetus obesus; from Gibson county, Indiana, Di- Gotyles nasutnn, found when digging a well between 30 and 40 feet be- low the surface; from tho INIiocene of the Bad Lands of White river, Dakota, Leptictis haydeni, Icfops dakotensh; from Half-moon Bay * Geo. of X. Jersey, 1868. t Proc. Acad. Nat. Sci. McHozoic iiinl (,'a:iio::oio Geoltxjij and Palivontuloyy. 221 Cjiliforniji, />el/»hintis oacitlKiis; from Wtisliiiij^lon coimty, TexiiM, An- chi/tpiis textniun; IVom tlio Hiitl LtunU of NobruMkii, Lojt/iioilon orcfden- t(ite,a\ul from Slwuk rivur, MoimioiiMi loiinly, New Jersey, Anchippo- di(.'< ripat'iiis, T. A. ('on ..(I* (losi-ribeil, from the Miocene of llie Atljinlie coast, Voliitdid ooi/ortni.s, Pratnim rifjlniann, now Afari/inelln vinjinuinu, Merceiiarkt cnnenta, Vanjatia p'tonenui, Carditanieni recta ; and from Wyomin<^', Goniohasin carteri. Prof. O. C. Marslif described, from tlie Tertiary nt Antelope station, on the Union Pacific Uailroail, 450 miles west of Omaha, in Nebraska, /'Jqinis ptiroiUim, now I'rotoliippnti jxtt'ou/its. The Tertiary nnderlics a wide central belt in West Tennessee, and was snbdivideil by Prof. Sallbrd,;); in 1801), in ascending oider, into 1, Porters' (Jroek Gronp ; 2, Orange Sand ; ;{, Blutf Lignite ; 4, Post- pliocene beds, on the; AIississip[)i IJlnff, consisting of Bhilf gravel and IJlulf loam ; and superficial gravel beds, in other parts of the State, consisting of ore-region gravel, eastern gravel, and lastly of bottoms, and alluvial beds. The IJluff lignite consists, especially in the middle and southern parts of the State, of a series of stratified sands, with more or less sandy, slaty clay, cluiracteri/ed by the presence of well-marked beds of lignite; though, in the northern part of the State, its upper portion is frequently more or less indurated, presenting la3'ers of soft sand- stone with less lignite. The upper part of the series is generally well exposed below the gravel of the Mississippi BlufTs. At ^Memphis, how- ever, it scarcely ai)peai's above low water. About one hundred feet of the series has been seen. In this thickness it contains from one to three beds of lignite, which are from half a foot to four feet in thickness. The outcrop of the Orange sand or Lagrange Group, forms more than a third of the entire surface of West Tennessee. It occupies a belt, about 40 miles wide, which runs in a northeasterly direction, through nearly the central portion of this division of the State. As seen in bluffs, railroad cuts, gullies, and in nearly all exposures, it is generally a great stratified mass of yellow, orange, red or brown, and white sands, presenting occasionally an interstratified bed of white. * Am. Jour. Conch., vol. iv. t Am. Jour. Sci. & Arts, 2d scries, vol. xlvi. I Geo. of Tenn. 222 Tertiary. Wr grey, or variegated clay. The sand beds are usually more or loss argillaceous ; sometimes but little, or not at all so. Like the Ripley Group, it contains, occasionall}^ patches, plates, and thin layeis of ferruginous, sometimes argillaceous sandstone, and as in that group, presents, locally, massive blocks of sandstone on high points. At La Grange, a fine section of the group, more tliau a hundred feet in thickness, is exposed. It includes within its outcrop, nearly all of Fayette, Haywood, Madison, Gibson, and Weakley counties ; the larger parts of Hardeman, Carroll, and Henry ; and small parts of Shelby, Tipton, Henderson, Dyer, and Obion. He supposed this group to be of Eocene age, and to have a thickness of about 600 feet. This group must not be confounded with the Post-pliocene Orange sand of Hilgard, which occurs in Mississippi and Louisiana. Tlie Porter's Creek Group contains proportionally more laminated or slaty clay than the Orange Sand or Lagrange Group. Along the Mem- phis and Charleston railroad, the belt of surface occupied by the group is about eight miles wide. It becomes narrower in Its north- ward extension, and appears to be the northern extension of the lower part of Hilgard's Northern Lignitic Group. The thickness is from 200 to 300 feet, and in this are usually several beds of slaty cla}' from five to fifty feet in thickness. It is well exposed on Porter's creek, in Hardem.ui county, and on the road from Bolivar to Purdy, commenc- ing about seven miles from the former place, and extending to or be- yond NVade's creek. Prof E. W. Hilgard'* described the Grand Gulf Group, Orange Sand and Loess at Port Hudson, Miss., and gave a descending section midway between Port Hudson and Fontania as follows: 1st, Yellow loam, sand}^ below, 8 to 10 feet. 2d, White and yellow hard pan, 18 feet. IJd, Orange and j-ellow sand, someiimes ferruginous sandstone, irregularl}' stratified, 8 to 15 feet. 4th, Heav^-, greenish or bluish clay, 7 feet. 5th, White, indurate silt or hard pan, 18 feet. 6th, Heavy, green cla}', with porous, calcareous concretions above, ferruginous ones below; some sticks and impressions of leaves, 30 feet. 7th, Brown muck and white or blue clay with cypress stumps, 3 to 4 feet. At tiiv stage of extreme low water the stump stratum is visible to the thickness of 10 feet at its highest point; showing several genera- tions of stumps, one above another, also the remnants of many succes- sive falls of leaves and overflows. The wood is in a good state of =•■• Am. Jour. Sei. v. Arts, 2d series, vol. xlvii. Mesozoic and Ccenozoic Geolorjy and Paleontology, 223 preservation. The stump stratum exists, at about the same level, over all the Delta plain of the Missij:sippi and along the Grulf coast from Mobile, on the east, to the Sabine river. Dr. Joseph Leidy* described, from the White River Group of Dakota, Oreodon affinis, O. biillatus, 0. hybrldini, Leptanche/ua nitida, Homo- cameltis caninus, Cosoryx furcatus, Nanohyus porcinus, Protohippus placidus, Hipparlon affine, and H. (jratum, lie described from the Eocene near Fort Bridgor, Wyoming,f Oniomys cartcrl, Trionyx guttatus, Emys wyomingensis. and from South Bitter creek, near where it crosses the stage route, 70 miles west of the summit of the Rocky mountains, in western Wyoming, Crocodilus apf.us. Prof. E. D. Cope;]; described, from the Miocene of Shiloh, Cumber- land count^^ Now Jersev, Tretosphys uvcens, Zarhachis velox, and Trionyx limn ; from the mouth of the Patuxcnt river, Maryland, Zarhachis tysoni. He described, § from the Eocene marl pits, at Shark river, Monmouth county, N. J., Hemicaulodon. effodicns; from Farmingdale, 3£yliobates glottoides, and Cmlorhynchus aciis; from the Green River Group, on the upper waters of Green river, Wyoming, Asineops squamifrons, Glupea pwiilla^ Cyprinodon levntus; from the Miocene in Wayne count}'. North Carolina, Pnemnatosleiis nahunticus; from Duplin county, Pristis attenuatus: from Edgecombe county, Eachrichtivs polyporus; from Quanky creek, Halifax count}', Mesoteras kerranus; from Stafford county, Va., Thinotherium annulatmn. He described, from the Post-pliocene, at Savannah, Georgia, Anoplo- nassa forcipata; from cave Breccia, in Wythe county, Virginia, Tainias IcBvidens, Sciurus panolius, and Galera perdicida Prof. 0. C. Marsh II described, from the Eocene, near Shark river, Monmouth county, New Jersey, Dinophis grandis. T. A. Conrad^ described, from the same localit}', Pecten Icneiskerni, Crassatella littoralis, Crassina veta, Biicardia vela, Cnryatis d ,la- toarensis, Protocardia cnrta, Onasfus annosns, and Terebratula glossa. And from the Miocene of St. Chai-les count}', Maryland, and from Petersburg, Va., Pecten cerinus, Callista virginiana, Saxicava insita, Scapharca tenuicardo, Mercenaria plena, and Capsa parilis. '■' Jour. Acad. Nat. Sci., vol. vii. f Proo. Acad. Nat. Scii. t Proc. Aoad. Nat. Sci. § Proc. Am. Phil. Soc, vol. xi. II Am. Jour. Sci. & Arts, 2d series, vol. xlviii. IT Am. Jour. Conchology, vol. v. 224 Tertidry. ■ I W. M. Gabb* described, from the Miocene in Contra Costa comity, near Tomales ba}', near INIartinoz, Walnut creek, Monterey county, San Emidio, Cerros island, and other places in California, Dosinia mntfiewsoiii, Pecten pdckkami, Tn'ptera clavdta, Trophon 2Jondero.suni^ JS^c/jtmiea recurca, 3fetula reiaondi, Agasomd yravicht, A. slnnata, liduella mathewsoni,, now Bursa iiidt.hetvsoni, Cunid hiplicdtd, Ancilldria Jishi, JS^everita cdllosa, Cdticelkiria vetiistd, TurriteUd hojfmduni, Trochitd Jilosd, T. tnorndtd, Pachypoma bid)iguldtd, Pandora scapha, Ileminidctrd lenticnlaris, H. occiden- tdli's, Schizodesmd abscissa, Chione mathewsoni, now CalUsta mathewsonf, 0. wh!f,ii.eyi, now C whitneyi, CalUsta voy>\ Dosinia conradi, Tapes truncata, Cardium nieelcandin, Conchocele disjuncta, Mytilns mathewsoni, Modiold viuUiradiata, now Volsella multi- rddiata, Pecten cerrocensis, P. veatchi, Ostrea atwuodi, 0. taylorana, O. vedtchi, O, cerrocensis, Aster ids remondi, Ficus pyriformis, F. nodiferas, Venus pertemds. From the fresh water Tertiary, or Plio- cene, on Snake river, in Idaiio Territory-, Mefania taylori, and Lithasia antiqiia ; from the Pliocene, near Santa Barbara, Humboldt bay, San Francisco county, Kirker's Pass, Sonoma county, and other places in California, Cancer hreweri, Snrcidd cdrpenterana, Pleuro- soma voyi, Colnmbella richthofeni, Littorina remondi, Zirphaid dentatd, Gdri alata, Dosinia sfxtleyi, now 'Jkipes staleyi, Cyrena cdlifornicd, Lucind richthofeni, Neptunea altispira, iV. hmnerosa, Siyavetus planicostum, Cancellarid altispira, Acmnia riidi'i, Siliqu- aria edentula, Caryatis barbarensis, Sdxidomns f/ibbosiis. And from the Post-pliocene, near Santa Bitrbara, and San Pedro, SiircHla fryonana, S. perversa, Clathurella conradana, Muricidea paiicivari- catd, Trophon squdinnlifer^ Cancellarid (jrdcilior, and C. tritonided. Prof. Leo. Lesquereuxf described, from the Lower Eocene or Northern Lignitic Group of Tippah, Miss., and La Grange, and Sommerville, Tennessee, Cdhirnopsis dandi, Sabal yrayana, now Sabalites yrayanus, Salisburia binervata, Popidus monodon, SdUx wortlteni, S. tdbellaris, Qaercus moori, Q. retrdctd, Celtis brev/foUd, Ficus schimperi, F. cin- namonioides, Ldurus peddtiis, Cinndmomum mississippiense, Persea lancifolia, Ceanothus meiysi, Juyldns appressd, J. saffordana, Mag- nolia laurifolid, M. Lesley dna, M, oralis, M. cor dif olid, Asimina leiocarpa, and Phyllites truncatus. * Pal.ofCal., vol.ii. t Trans. Am. Phil. Soo., vol. xiii. Mesonoic and Coniozoic Geolot/y and Pahvant oingy. 225 Oswald Heer* described, from the Tertiary of Alaska, Pterin sitken- sis, Taxodinm tinajortini, Taxites mi.crophijllus, Pliragmites alaskanun, Poacites tenui'striatus. Carex servata, Sagittaria palchella^ Vacciniiim frie)i\ Di'ospy ros stenosepala, Vihvrnnm nordenslcioldi, Redera avri- culatn, Vitis crenatn, Tilia alaskana, celasfrvs horealis. Ilex insuj- nis, Traj)a horealis, Jmjlans nigella, J. picroides, Spiraea andersoni, and identified numerous plants with those described from the iSliocone of Europe. lie described the insect CJir;/somelites alaskanus, and Dr. Carohis JMayer described, Unio ona-'otis, U. athlios, Paludina abavia^ and Melaniafuruhjelml. The Jackson Group, in Louisiana,! consists of marine strata; of lig- nitic beds that tell of swamps; and of noufossilifcrous beds of lamin- ated sands and clays. It spreads over the State north of the Vicks- burg outcrop and west of the Bastrop Hills. The marine strata con- tain massive clays, often full of selenite. At Grand View there is a stratum of such clay 85 feet thick. The Vicksburg Group, in Louisiana, consists of smooth, yellow and red clays, with a very small proportion of sand. Limestone no- dules occur, generally, soft and yellow, but sometimes liard and white, and always full of casts of shells. It is exposed from Godwin's shoals to about six miles south of Natchitoches, and from a point below Montgomery to the Washita, below Grand View, but it never occupies an area more than about twelve miles wide. In 1870, Dr. Joseph Loidy;]; descrilied, from the Fort Bridger Eocene, of Wyoming, liaptemiis logomingensis, now Dcrmatemys wyoming- ensis, Emys stevensonnnus, Palriofelis ulta, Lophiodon modestns, Ilyopsodus 2iatiJus,Umys jeansi. E. haydeni, Baena arenosa, Saniva ensidens ; from near the junction of the liig Sand}' and Green rivers, Palmosyops paludosus, Crocodilns elliotti ; from Black's Fork, Microsus cuspidatus, NofharoAns tcnebrosus ; from the T'ltiary of Colorado, Megacerops aoloradoennis ; from the Tertiary .^r ttie Rocky mountain region, Oncot)afis pentagon its, Mylocy- prinufi robustiis ; from Henry's Fork of Green river, Lophiotheriuni syli-aticmn ; from the Miocene in the valley of Bridge creek, a tributary of John Day's river. Oregon, Oreodon s'lfperbns, Jnchitheriinn condoni ; from Gay Head, Martha's Vineyard, Graphiodon vinearius ; from the * Flora Fossilia Alaskana. T Goo. of Louisiana, 1870. t Proc. Acad. Nat. Sci. 226 Tertiary. ' \ Pliocene of the Niobrara river, 3Ierychoch(erus rusticus ; from Dry creek, Stanislaus county, California, Mastodon shepardi ; and from Tuolumne county, Anchenia cnlifornico. Prof. O. 0. Marsh* (lescril)O(l, from the Eocene of New Jersey, The- cachainpsn minor; from the Miocene of Edgecombe county, North Car olina,t Cnfarrnctes antiqaus; from Maryland, Pufflnus conradi; from the Niobrara river, Grns haydeni, Graculus idahensis; from Squan- kum. New Jersey,;J; Uhinoceros matuti'nn.i; from Shark river, Dicotyles (i.ntiqnun; and from the Pliocene at Monmoutli, Meleacjris alttis. Prof. F. B. Meek described, fi'om the Miocene, at F'ossil Hill, Hot Spring mountains, Idaho, Spharium rirgosum, S. idahoense, Ancyius unduIatKS, Ooniohasis sculptilis^ O. subsculptilis, Carinifex hinneyl, C. concava and C tryoni. T. A. Conrad§ described, from the Miocene of Virginia and South Carolina, Artena inididata^ Crepidula rostrata, G. recurvirostra, C. virflinica, Persictda ovula, and Axinwa bella. The Grand Gulf Group of Louisiana! consists of nonfossiliferous cla3's and sandstones pretty regularly stratified, A^aried, occasionally, by claj'e}- sand and beds containing twigs and leaves. The sandstone oc- curs in ledges from six inches to 20 feet in thickness. It is cut into four parts by the bluff and the alluvion of Red river and the Missis- sippi. One reaches the Vicksburg area and extends into Missis- sippi; another is southwest of Red river and extends into Texas; an- other is northeast of Red river as far as Sicily Island on the Ouachita; and the other is at the western part of the Avoyelles prairies. In 1871, T. A. Conrad*[ described, from the Eocene a.t Claiborne, Alabama, Garyatis exigaa ; and from the Oligocene at Vicksburg, Mississippi, Macoma snblintea, and Abra protexta. F, B, Meek** described, from the Bridger Eocene at Henry's Fork, Black's Fork, and Church buttes, Wyoming, Viviparus loyomingensis. Brady and Crosskeyff described, from the Post pliocene of Port- land and Saco, Maine, and from INIontreal, Canada, Gythere mac- cJiesney/', G. loyani, G. cuspidata, Gytherura crisfata, G. gninidosa^ and Gytheropteron complnnatiDn. * Am, Jour. Sci. aiul Arts, id seriL-s, vol. 50. f Ibid, vol. xUx. I Proc. AcaU. Nat. Sci. $ Am. .Tour. Conch., vol. vi. li Geo. of Lou., 1871. IT Am. .Jour. Conch., vol. vi. *'•• Proc. Acad. \at. Sel. tf Loud. Geo. Mag., vol. viii. Mesozoic and Coinozoic Geology and Palaontology. 227 Dr. Joseph Leidy* described, from the Bridger Eocene of Wyoming, Anostcira ornata, Hybemys arenarius, Testudo corsoni^ Emys carteri, Baena undata, Troyosus vetulus, now Anchippodiis vetulus, Sinopa rapax, Paluiosyops major, Hyrachyus eximius, Paramys delicatus, P. delicatior, and P. delieatittsimus, all now Plesiarclomys, and Mysops minimus. He described from the Miocene of Alkali flats, Oregon, Bhinocerns pacijicus.^ and from Crooived river, Stylemys oregonensis, now Testudo oregonensis. * Prof. E, D. Copef described, from the Post-pliocene occurring in a limestone fissure in Cliester county, Penns\'lvania, Megalonyxloxodon, M. sphenodon, M. tortulus, M. wheatleyi, Sciurus calycinus, Arvicola speothen, A. tetradelta^ A. didelta, A. involuta, A. sigmodus, A.hiati- dens, Erithizon cloaciiiiim, and Praofkeriumpalatinum. He described from the Miocene near Tuxtla, Chiapas, Mexico, Prymnetes longiven- ter. Prof. O. C. MarshJ described, from the Green river basin west of the Rocky Mountains, Boavus agilis, B. brevis, and B. occideatalis; from the Bridger Eocene of Wyoming, Limnophis crassus, Lithophis sar- yenti, Crocodilus affinis, G. brevicollis, C, grinnelli, C. liodon, C. zipho- don, now Limnosaurus ziphodon, Qlyptosaurus anceps, G. nodosus, G. ocellatus, G. sylvestris, Titanothcrium (?) anceps, Lophiodon affinis, L. bairdianus, L. nanus, L. ijumilis. Anchitheriam gracile, now ( ?) Orohip- pus gracilis, Lophiotherium ballardi, Elotherium lentum^ Platygonus ziegleri^ Hyopsodus gracilis, Limnotherium elegans, L. tyrannus, Sci- uravus nitidus, S. parvidens, S. undans, Triacodonjallax, Canis mon- tanus, Vulpavus palustris, and Bubo leptosteus. He described from the Miocene at Scott s Bluff, on North Platte river, Nebraska, Amphicyon angustidens; from Northern Colorado, Meleagris antiquus; from Cumberland count^^ New Jersey.g Lophio- don validus, now Tapiravus validus; and named, but did not describe, from W^'oming, Aniia depressa, A. newberryana, Lepidosteus glaber, and L. whitneyi. Also from the Pliocene sands, near the headwaters of the Loup Fork river, Nebraska, (||) Platygonus striatus, Arctomys vetus, Geomys bisulcatus, Aquila dananus; and from Oregon, Platy- gonus condoni, and Dicotyles hesperius. * Proc. Acad. Nat. Sci. + Proc. Am. Phil. Soc, vol. xii. t Am. Jour. Sci. and Arts, 3d series, vol. i. . A lonjj;, lint riiljio ('XtciidH down a little east of nortlMVoin tlio Uinta tnouutiiins. betwocn Hhick's I'ork and the Muddy. Tliis may ho regarded as tlio ^'colo-j^ical divide lie tweeii the watcM's of the (Jreat Salt Lak>' Hasin aiid the di'aina^e of (Ireen river. The Muddy is one of the hranehes of Hlaek's l-'orU, whieh llowH into (Jreen river, and west of this .stream we have what is ealled the eastern rim of the Great IJasin of Salt Lake. If we wen- to travel soutlnvard to the foot of the Uinta moiititain.s, from the rail road along this divide, we should be able to dcteet no well-marked line «)f se|)aration between the (Jreen River rtroup and the W'asateh (Jroup. Hridger's IJutte, as well as the entire eastern [jortion of this divide fronting the valley of Black's Fork, exhibits a large thickness of the .somber, indurate'd sands, clays, and sandstones of the Ibiilger Group, passing down into light buff, chalky layers, with Plunorbis, Unto, He- lix, Goniohasls, etc. Within a distance of ten miles to the west of this l)utte the little streams cut through the V''dcish beds of the Wasatch Group, then pass up into whiter, indurated, marly clays, with numer- ous concretionary layers, uiflering from the chalky beds of the liridger and Green river basin. This divide probably forms the junction of two great fresh-water lake basins, that may have existed contemporane- ously. The two great basins may .have been connected with each other at different points at some stages of their growth, but there is an abrupt, persistent, very marked difference in the character of the sediments of the two basins. While the Green River and Bridgei- Groups abound with fossils, the Wasatch Group, like all the rocks of the west that are characterized by brick-red coloring matter, is compara- tively quite barren. At Bridgcr station, and from Hridger to Aspen, which is about 24 miles, the ochreous beds of the Wasatch Group are well exposed on both sides of the road, and the valley through which ^ the road passes from Piedmont to Aspen is carved out of this Gron[) The tunnel at the head of Echo canon is cut through the reddish and purplish indurated sands and clays of the Wasatch Group. It is 770 feet in length. The valley of p]cho canon is one of erosion, and on either side the rocks rise wall-like 500 to 1,000 feet, or have been weathered into curiously castellated forms, a)ul bear such names as '?! 23G Tertiary. . (■■ Witches' Rock, Eagle Rock, Hanging Rock, Conglomerate Peak, Sen- tinel Rock, jMonument Rock, etc. Monument Rock is a regular obelisk of conglomerate, standing at the junction of the Echo with the Weber valley, and being about 250 feet high. Descending the Echo canor , the more rugged picturesque scenery- is exhibited on the right hand, and descending the Weber the same lofty perpendicular walls^ weathered here and there into all sorts of fantastic forms, continue to the Narrows, where the Weber river makes a bend to the left, and the conglomerates disappear. The whole series of these beds is referred to the Wasatch Group, and the thickness estimated at from .3,000 to 5,000 feet, the conglomerate portion being from 1,500 to 2,000 feet. He proposed the name of the "• Sweetwater Group," for a lake deposit found in the Sweetwater valle}-. There is a high ridge or divide, between the drainage of Wind river. North Platte, and Sweetwater, 300 to 400 feet above the channels of these streams, which is com- posed of the Tertiary beds. The Sweetwater forms a distinct concavity, with this high divide on the north and east, and the vallej' has been scooped out so that until we roach the Sweetwater Canon, near the South Pass, only the massive granite ridges rise up among the modern Tertiarj^ beds, which jut close up against their base. This is a valle}' of denudation, over a space of at least 30 to 50 miles in width. All the unchanged formations, from the lignite Tertiary down to the massive feldspathic granites, have been worn av-'a}', leaving the granites scat- tered over the valley in the isolated ridges. At that time there was w fresh-water lake which occupied the entire valley, ni'ich as Salt Lake once occupied the great basin, concealing most of the granite ridges, while others rose above the waters like islands. Then was de posited what he called the Sweetwater Group, or perhaps a series of beds identical with the upper portion of the WinIissis- sippi in descending order, into, 1st, Vicksburg Group, 120 feet; 2d, Red Bluff Group, 12 feet; 3d, Jackson Group, 80 feet; 4th, Claiborne Group, 60 feet; 5th, Buhrstone Group, 150 feet; Gth, Flatwoods and Lagrange Lignitic Group, 450 feet, making a total thickness of 872 feet. The Lagrange and Porter's Creek Group of Saffbrd is the same as the Flatwoods and Lagrange Lignitic. The Buhrstone Group of Tuomey is the same as the Siliceous Claiborne Group of Hilgard. The Eocence is followed by the Grand Gulf Group, probablj- a de- posit in brackish wat^r, almost non-fossiliferous, and having a thickness of 250 feet. Prof. Leo Lesquereuxf described, from the Green River Group of * Proc. Am. Ass., Ad. Sci. + 1872, IT. S. Geo. Sur. of Montana, etc. Mesozoi'c and Cwnozoic Geologif and PalcBontologij. 23:1 W^'oming, high on hills from the river, Ceanothus cinnamomoides, now Zizyphua cinnamomoides ; from the liridger Group at Washakie station, near Bridger's Pass, Rhamnus intermedins, Liqnidnmhar (fracile, now Aralia gracilis, and Quercus (emulans; and from Barrell's Springs, Equisetum haydeni. After reviewing the state of the knowledge of the Tertiary and Cre- taceous flora of this country, he arrived at the following conclusions, to- wit: 1. The Tertiary flora of North America is, by its types, intimately related to the Cretaceous flora of the same country. 2. All the essential types of our present arborescent flora are al- ready marked in the Cretaceous of our continent, and become more distinct and more numerous in the Tertiary; therefore the origin of our actual flora is, like its./rer Group ol' Hitter creek, and Cottonwood creek, Limnohyns loividens; from a bluil on Green river, near the moutli of tiie Big Sandy, Wyoming, Pnlfcosij- opafontinalis; from the summit of Chiircli Butte, Trionpx hetero(ilyi)- tus;\ from the Bad Lands of Cottonwood creek, T. scntaiiiantiqmim. Pcvppichthys plicatus, P. sclerops, P. Icvis, P. symphysis^ Rhineastes mdidus ; from Ham's Fork, liffua ponderosa, Clnstes anax ; from tiic Green River Group, near Evanston, U':ah, Bathniodon latipes ; from near Black Buttes, Emys euthnetifs, E.meyaulax, E.pachylomits; from Upper Green river, Pappichthys corsoni, lihineastes c(dvt(s, li. arciin- (Hs; from (Treen river basin,;}; Antincodon furcatus, now Sarcolemnr fnrcatus, Orotherinm (now Hyracotherium) index: from Cottonwood creek, 3Iicrosyops vicarius, OUgotonms cinctus ; from South Bitter creek, Paramys leptodns, Eobasileus galeatus, Achwnodon insolens, from irenry's Fork, Palmosyops dlaconas, Hyrachyas implicatus; from near Evanston, Phenacodiis primcBviis. He described, from the Miocene of Colorado,^ IJyopsodus mini- mus, Hypertragulns calcaratus, II. f.ricostfitas, and 3Ienof.herium h-murinum: from the Miocene of the Western plains,| Aelnrodon mus- felimns, now 3fustela pai'viloba^ Aphelops megalodus, PolcBolagus (Kjapetillus,^^ Colotaxis cristatus, Ilyrocodon quadriplicatas, now An- chisodon qnadripUcatus, II. nrcidens, Symborodon tomts, Miobasile- vs ophryas, 3fegaceratops acer, 31. helocerus, Peltosaarus granulosus. Testndo amphithorax^ T. cultratus, T. laticunens, T. ligonius, Domnina gradata.** Ilerpetotherivmfugax, Daptophilns squalidens, Tomarctus brevirostris, Sfibaru obtusilobus, Cants gregarius, Isacis (now 31 io- dectes) caniculus, Paloiolagus triplex., P. turgidus, Tricium avunculus. T. leporimnn, T. pauiense, Gymnoptychns minutus, G. nasutus, O. trilophus, Anchitherium cunentum, and I'rimerodus cedrensis. Prof. O. C. Marshf t described, from tlie Eocene deposits of Wyoming and Oregon, Dinoceras mirnbilis, Orohippus agilis, C'olonoceras agres- /is. Dinoceras lucaris, Oreodon occidenfalis, Rhinoceras annectens R. oregonensis. Tillotherium hyracoides ; from tlie Afiocene of Colora- * Proc. Am. Phil. Soc, vol. xiii. t U. S. Geo. Sur., Wyoming, etu. I Pal. Bull. vol. xii. 'i Proc. Acad. Nat. Sei i Pal. Bull. vol. xiv. If Pal. Bull. No. XV. *'■' f»al. Bull. No. xvi. tt Am. Jour Sei. and Arts, :id ser,, vol. v. m Mesozoic and Ccenozoic Geology and Paloiontology. 243 do, Brontotherium gigns, and Elotherlum crassum; and from the Up- per Eocene of Wyoming',* Dinoceras laticeps. Dr. Joseph Leidyf described, from the Bridger Group in the Buttes of Dry creeii, Ilgopsodus mimtscidus, Mgsops fraternus, Wa '■' U 24 S Tertiary. ii liicustrine formation of Eoccno aj^c, thoui^h liaviiig (ixaininod an out crop for forty miles, he (li.scovcred no fossil remains except fossil wood, lie said the material is so easily transported tliat the draina immediate valley of the Piierco to a point eighteen miles below Nacimiento. This section of the Eocene strata in the region west of the Sierra Madre Range in New Mexico consists of green and black marls, which he named the Puerco Group, fjOO feet; sandstone of the Wasatch Group 1,000 feet, and red and gray marls of the same group, 1,500 feet; mak- ing a total thickness of 3,000 feet. He described,* from the Eocene of New Mexico, Ambloctoniis nin osus, Protctumus secundnrius, P. muUicuspis, P. strenuiis, Diacodon alticuspis, D. coilatus, PcUjcodus fruyivorus, Paatolestes chacennis, Opisthotomus astutvx. 0. Jlagrans, Aniiacodon nientalis, A. crassun, Hyrachiitis sirifjularis, Hyracotherium lapirinum, H. angu'jtidens, II ^ nuspidatam, Buthniodon latldens, B. cmpidtdus, Diplocynodus sphenovs, Crocodilus grypus, C. wheeler i, and Dermatemys (/) costilatas. He described,! from the Miocene of Cumberland county. New Jersey, Phasyanodus gentryi, Sphyr'tmodus silovianus, r/nl Ayabelvs porca- fiis ; from Flowei's T oar! pit, Duplin cinty, Noifch Carolina,;!; Pristis attenuatus ; from Edgertoa's plantation, in Way no county, Pneiima- tosteus nahnnticus ; from Halifax coualy, MescMras kerrianus, ami Delphinapterus orcinus. From the Loup Fork Group of New Mexico,^ Pliauchenia humphreysana, P. vulcanorum, Hippotheri- urn calamarium, and Aphelops jenezanus ; and from the Pliocene of- the West, Canis ursinus. Prof O. C. Marsh|| described, from the Eocene of Wyoming, Lemi(- ravus duitcws, Tillotherium fodiens ; from Utah, Diceratherium ad- venum, Diplacodon elatus, Orohippus uintensis, and Agrinchcerus pamUns. From the Miocene bad lands of Nebra'^ka, Laoplt/eciis ro busius, Anisacodon montnnus ; from the John Day rivet- in <)i'egon, * Geo. Sur. W. 100th Mnidian, Syst. Catal . of Vertobiutu,. t Prof. Am. Phil. Sci. vol. xiv. X Geo. of N. Carolinn. I Troa. Acad. Nat. Sci. II Ain. .Jour. Sci. and Arts. 3d ser., vol. ix. I Mesoznir, and Ctnnozofr Ovoloijif (uul PnhvotUoloi/y. 240 vvluMo the beds liiiv(! an cstinmtcd lliiclviicss of r),()()0 (Vet, Ih'c.crathcri- am firuuffum, 7). /irnnim^ Thituthijus lenfiis, iiiul 7'. socialt's. 'l\ A, Coiii'jul* (lescrlbeil, from tlic Koecno iit Wiltiiiiifxtoi), North Caroliim, Terehntfidn demissirosti'ti; hikI IVoiu lU'juil'oit, Pecfen (ini- soplenra and P. cnrolineiisis. From the MioccMU' near VVilminyton, and other placets in Nortli ('ar- olina, Liropecfcn cat'ofinoisis, Os/reti pcrlirafa, P/dciinonn'a Jrar/osn, lincta (ilfe red Wasatch beds at the base, the line of division can be distinctly traced, descending somewhat in horizon toward Barrel springs, and ascending again beyond toward Cathedral bluffs. A section taken at Sunny Point, near Little Snake river, gave a thickness from the river to the summit of the cliff' of about 2,000 feet. The upper 'J50 feet belonging to the Green river series, and the remaining 1,050 feet to the Wasatch Group. The Green Kiver Group is exposed in the valley' of Brown's Park, which is a bay-like depression, from 6 to 8 miles in width, occu- pying the geological axis of the eastern end of the Uinta mountains, from 1,000 to l.,200 feet in thickness. Throughout the valleys of the Little Snake and Yampa rivers, these groups have been worn into rounded ridges, where, generally, only disintegrated material is found. In the basin of Vermillion creek, thebcils of the Wasatch Group have their greatest development. It was on one of the broad benches, be- tween the branches of this creek, to the east of Rub}- Gulch, that the originators of the famous diamond fraud, of the summer of 18711, lo- cated their pretended discovery. An exposure of coarse, iron- stained sandstone, on the surface of the mesa, at the foot of Diamond Peak, was strewn by them with rough diamonds and rubies, which were in- Mesozoic and Ccenozoic Geology and PaUtontology. 257 I r If genioiisly mixed with tlie soil around, so as to make it appear that they came from tlie decomposition of the sandstone. Along Bear rivei-, in Utah, from Bear River City to Evanston, the hills on either side are occui)ied by the nearly horizontal beds of the Wasatch Group. The greater part of Bear river phiteau is covered with a considerable thickness of these beds, which are in general rather coarser and more conglomeratic than those of the Aspen plateau. Its summit varies in width from 2 to 4 miles, beyond wb.ich to the east- ward these beds are oxposed in the deep canons of Woodruff, Randolph and Saleratus creeks, from 2,000 to 2,800 feet in thickness; He found the Savory plateau region covered, principally, b}' hori- zontal beds of the North Park Tertiar\', which he referred to the Plio- cene, and which, as proved by exposures in the deeper cuts, on its northern edge, overlie tlie upturned edges of Cretaceous and earlier beds, while the higher portions of the ridges are capped by remnants of the Wyoming conglomerate. The best exposures are found in the open valleys at the heads of Savory and Jack's creeks, and on the pass between the Archaean body of the Grand Encampment mountains and the Savor}^ plateau. A thickness of not less than 1,000 feet of these beds is here exposed, which is made up in the upper portion of a thickness of about 300 feet of a 'Irab, earthy, somewhat porous, lime- stone, sometimes inclosing small pebbles, underlaid by beds, wliich grade off insensibly from lim^- sandstones into coarse gravel beds. They occupy the valley of the North Platte to the South of Jack's creek, forming long, gentle slopes, extending up from the river to the flanks of the Grand Encampment mountain, which, thougii so covered b}' recent deposits that only few exposures of the underlying Tertiary are found, suflicientl}^ show the continuity of their original deposition. Their beds may be traced along the line of bluffs bordering the vallc}' of Sage creek on the south and west. Here the upper member is a hard sUicious.shale, more like an older rock, under which are seen the white limy sandstones ; the lower beds being concealed beneath debris accumulations. Arnold Hague found the Whit^ River Group along the south and east face of Chalk bluffs, in Wyoriing, resting unconformably upon the Laramie Group, and protruding from beneath the Pliocene beds. The strata are exposed near Carr's station, on the Denver Pacific Railroad, eastward across Owl creek, the tributaries of Crow creek, and beyond. The thickness of the group is estimated at 300 feet, and is of Miocene age. Pfp 258 Tertiary. I' > ' \^ % f I . He estimated the thickness of this Pliocene lake strata, which he called the Niobrara Pliocene exposed in Wyoming, at from 1,200 to 1,500 feet. The beds are found lying unconformably upon the older uplifted strata, and overlapping the area of the Miocene basin. South of the Union Paciiic Railroad, they occur abutting against Mesozoic foima- tions; just north of Granite Canon, they lie next the Archaean mass ; and a short distance beyond, at the mouth of Crow Creek canon, are found essentially horizontal against nearly vortical Palaeozoic lime- stones. From Crow creek, northward, they may be seen resting direct- ly upon every formation, from the Ardnean to the Fox Hills Group. The strata consists of marls, clays, coarse and line sandstones, con- glomerates, with some nearly pure "limestones. Fine, marly sand- stones are .the predominant beds. Overlying the Pliocene lake deposits on Sybille creek and its tribu- taries, and in the region of Chugwater and Pebble creeks, tliere occur beds of coarse and fine conglomerate, having a thickness of DOO or 400 feet. These beds have been called the Wyoming Conglomerate. In North Park, Pliocene beds lie unconformably upon the older rocks, resting in places against every formation from Archuian to the top of the Cretaceous, and are seen in undisturbed condition resting against the basalts. They extend over the entire Park basin, giving it the level, prairie-like aspect, which it presents from all the higher elevations. He referred the Tertiary beds in the eroded basins and valleys worn out in the rhyolite in the Toyabe range of the Nevada basin, and noticable on Silver and Boone creeks to the Truckee INriocene. S. F. p]mmons found the same formation in the valley of Reese river, near Ravenswood Peak, along the foot hills, both to the east and west of the Soldier's Spring Vallej' basin, in the low depression of Indian valley, and in the re-entering bay north of Black Canon, with a thickness of over 700 feet. The Truckee Miocene is so named from Truckee range, Nevada, which extends in a north and south line for 72 miles, and consists, for the greater part of the distance, of a single narrow ridge, barel}' more than 5 miles from base to base, but widening considerably at the southern end, where it is made up of broad fields of Tertiary eruptive rocks. Alfred R. C. Selwyn said* that between Blackvvater and Stewart's '•■ Geo. Sur. of Canada. Mesozoic niid Ctvnozoic Geoloyn and Palcboiitoloyy. 'J)\) Lake, and thence to the Finlny Rapiils, on Pence river, the country, with some exceptions, is more or less overspread with drift material ; much of this lias been derived from the abrasion of the Tertiary for- mations, tlirough which many, of the principal valleys of the country iiave been cut, exposing alternating beds of clay, lignite, sand and rounded gravel, capped b}' vast sheets of volcanic; products, chlcitly porous and compact lavas — columnar and concretionary — and dense dolerite, forming high hills or undulating st.iny table-lands, such as that which is crossed by the wagon road between Clinton aiul Bridge creek, at an elevation of 4,000 or 5,000 feet. From Mr. Horetzky's description of the abrupt character of the country on the iSusqua river, and in the vicinity of Fort Stager on the Skeena, these Tertiary volcanic products are supposed to be extensively developed in that region. The lignite Tertiary strata which are assumed to have pre- ceded the latest of these volcanic outbursts, occupy undefined, but ex- tensive ;ircas between Fort George and McLeod's lake ; and probably continue thence lo the valley of Nation river, with only such interrup- tions as are the result, partly, of the original unevenness of the sur- faces upon which they were laid down, and partly of the subsequent de- nuding agencies to which they have been subjected, giving rise to out- crop[)ings of the older rocks, either as hills or ridges rising above the general level of the country, or appealing as rocky bars or canons in tiie deep-cut channels of the rivers. The general similarity of some of the sands and gravels of the drift period to those of Tertiary age, makes it difficult, without close and critical examination of each ex- posure, to determine to which period they should be referred, and the distribution of the drift upon the Tertiary deposits is so irregular as to make it quite impracticable to define their respective limits. At about three miles below Nation river, a steep cliff rises on the right bank of Parsnip river, from the water's edge to 70 or 80 feet. At the base, stiff blue clays are seen, and these are overlaid b}^ la3'ers of sand and fine gravel, passing at the top into coarse rounded gravel. This is, probably, near the northern limit of the Parsnip river lignite- Tertiary basin, as a short distance further a rocky ridge crosses the river and crops out in both banks, the country then rising rapidly, on one side to the Rocky mountains, and on the other to the watershed between the Omineca and the Parsnip viveis. On the eastern side of the mountains there do not appear to be any deposits which can be re- ferred with certainity to the lignite-Tertiary series. At intervals along the river, on both sides, deposits of stratified sand and gravel, cut into Ml 200 Tertiary. benches imd terraces, extend from the water to elevations of seven or eijjht hnndreil feet. Somewhat similar sands and gravels are thinly spread over nian}' parts of tiie great [)r!iirie platean, which stretches eastward from the base of the mountains. A section of tiiese, about thirty feet thick, consisting of bn»wn sand, and reddisij rusty-looking gravel in thin bands, is seen ca[)ping the ste('|) hill of I'orizontal Cre taceous shales and sandstones, whii-h iises to an clevatictn of 550 feet above the rivei', immediately in rear of the Hudson bay post at Dun- vegan. In these high gravels the pebbles arc small and pretty uniform in size, in which respect they seem to diller from those of the lower benches, which are much co.'vrser; the small ; iid large pebbles being irregulaily distril)Uted through them. These u[)per gravels can not well be distinguished from those which, near Quesnel, occupy a position immediately beneath the basaltic lava Hows, and perhaps they belong to the same epoch. George 31. Dawson said that along the foot of the bank of the Fraser river, in front of the town of Quesnel, a considerable thickness of the lignite-bearing formation is shown. The lowest seen is situated about a mile above the confluence of the Quesnc ith the Fraser river, and consists of impure lignites and days with layeis of soft sandstone and ironstone concretions. These are followed in ascending order by clays and arenaceous clays of pale-grayish, greenish and yellowish tints, with a general southward or sonthwestward dip at low angles. These fill tiiy have been eiit iiwuy, ex(»'ii(l from th<' lower portion of the (/hileotin river we^twiird to thiit ptut of the Chihmco due sonUi of I'lint/ hiiie, on lh<' r;hilco, lo !i point Ji tew niiUis went of the lOUh meridiiui, iiiiil on the ChiK'otin itself, may stretch to Chizient lake, and thenee extend north- eastward, their boundary nearly foUowinif the Cluseo river for some distniH'P. They characli i izc the j^reater [)art of the Nazeo valley, and the pL'itetui extending east and west from it, and probablv reach the western slope of the range; of hills crossing the lilackwatei- at the upper canon. The rocks exhibited in these Hows ai'c usually true basalts or doleritcs of various V \tures, and from irongra}- to dark greenish and nearly black coUus, and often contain much olivine. The vesicles are comparatively seldom llUcd with infiltrated minerals, though near tile sources of the Na/co they are abno-t invariably so, the nuiterial being pale clialcedony, passing over in some instances to elirysopraze. In this vicinity, and near (Jinderella mountain, some l)eds are wacko like and scoriaceous, and the soil of the water shed region b 'tween tlu! Nazco and Bae-zae coh. on the Cluscu trail, seems to l)o almost entire- ly eom|josed of line rusty pumicous fragmcntJi. Samuel IT. Scudder (lescril)ed, froui a very fine grayislj and greenisli white lire-clay, in thin layers, with coniferous and angiospermous leaves .and seeds, 8,V inches thick, which is sui>erimposed upon a two- inch layer of carbonaceous clay, or imi)ure lignite or matted leaves, mingl(!d with clay, and succeeded by Wi) feet of sands and clays, at (^uesnel, the following insect remains, to-wit: Formica (ircnnn, JlypocJinia ohliterdta, Aphcunoyiistcr loiuffcva, PivipUi decessa, P. so.vea, P. se/iecta, dalyptitcs iintedUnvkuium, Bolettna sepiilta, Bracliijpezn obita, Ji. procern, Trichorifn dawsoni^ Anfhomyia inani- maffi, A. hitrifessi, Ilctcvomyza soi/lis, Sciomyza revelafa, Lilh t'trdis pictri, LoDchnta .seuesceiis, PaJ/ojitero morticina, Pi'ometopid dcpih's and Lfichtiiis petruruni. Roliert Bell, in his report on an exploration between James bay and lakes Superior and Huron, says, that in the region about the height of land, at the head of the east branch of the Montreal I'iver, the lower levels are fdled with gieat mounds and steep ridges of gravel and cobl)le-stones. The valley of this river, for some miles boff»re it joins the main stream, is also cover- il with similar materials. 'J'lic first limestone pebbles were observed on the MaLtagami, 24 miles below Kenogamisse Lake. Along the Mif^sinibi river, for many miles above its junction with the Mattagami, a blue clay, onh' occasionally holding :i62 Tc,t'fi;ht of 450 feet. Ainon<«- the fossils collected .are, 1th ipw lumen a ps'ittdceo^ Led rocks is often roundly sinootiied and striated as if produced by coast-ice acting in a rising area. Prof, E. D. (>opef described, from the shaleu of the Green River Group, Wyoming, near the main line of the Wasatch mountains, Dape- doylosxKS testis, Diplomystus denfntiis, D. analis, D. pectorosiis, I'Jris- inatopteriis endlirhi, Amplii.pl fiQci In'achypterd, Asineops pancirddidtHs, MioplosHs dbbrevidtus, 31. Idbracoides, M.louf/iis, M.bedni, Priscacard serrata, P. cypha^ ai-id P. Hops; fr(»m the Eocene of the Rock^* moun- tain s,| Cldsfes Uf/atiKs, Trioni/x rddulus, T. ventricosus, Pldstomenns stridlis, Stypolop/iHs hians, Tomifherium tiifmn, Plesidi'ctomi/s baccd- tus, Coi'i/phodon obliquus, C. lobdtus, Orotherium loewi; from the Loup Fork Group, Canis wheeleranus, Dicrocerus trildterdlis, and D. teh minus; from the Eocenej^ in Macon Co., Ga., Amj)hiemijs oxy sternum; from the Upper Miocene of Montana, Pithecistes brevifacies, Brdchy- meryx feliceps, Cyclopidius .si7nus, C heterodon, Blastomeryx bore- al is ; from the Loup Fork Gi'oup of Northwestern Kansas, /t/cotyles seri(s, Tetralophodon cdmpesler ; from the Pliocene of Oregon, (Jervus fortis, Anchybopsis altdvcits, A. anynstdrcas, A. (jibbarcus : from Washington Territory, Taxiden sidcata ; from Southwestern Texas, Psendemys bisornxttus, Cistudo mdrnochi, Anchybopsis brevi- nreus, and Cd;nobasileus tremon tiger us. '•■• Geo. Mag. 2d ser., vol. iv. t Bull U. S. Geo. Sur. Terr., vol. iii. t Wheeler's Sur. AV. 100th Mer., vol. iv. I Proc. Am. Phil. See. Jlfe.voi'o/c iind Cumozoic Ov.oloyy und Pdlifonloloijy. 2m I'rof. O. C. Miirsli* (loscrilKMl, from tlu; Miocene of llu- Kcuky moiin- lain rej4i()ii, Mot'opns (fisfdiis, M. senex, ami A/loiui/n nifviis; iVoiu tlie Tireeii Uivor Groiii) of VVyoininu, UeliolKitns nuliunn; :iii(l fnini the I'lioefsno of tlie Uoelvy nioiiiitaiiis, Mitt'opus e/ntuH, Tapiraons nwuxy Hinoii/erox, li. (il/eiii. tind CrocoUilus .solnris. I'rof. I'\ 1{. Meekt deserihcil, from tlie .Mioceneiit Cuclic valley, Utulu LiiniKva /I'iiKjL Di". ('. A. Wiiite| (les('ril)e(l, from tlu; VVtisutcli (ri-oiif) at Hlaek Hiittes Station, VVyoinin;^;, Unio proritii.s, ff. hol.iii".n(tiiiis, U. cudUcki^ U. conesi ; and iVoni Wales, in Utah, and the 'Janon of Desolation, of Green river, (fiiio meudax ; iVoni the Tertiary,,; at Last Blutl", Utah, I*hi/.sa pleuromaUs ; and from Joe's Valhiy, Vi'vipdnts iotncus. In 187S, Prof. C. A. \Vhite|| said the VVasateh Gi')iip is the lowest q^ a series of three freshwater Tertiary Gronfis, all of wliii!h are inti- mately connected, not only liy an evident continuity of sedimentation thronghont, but also by the passage of a i)ortion of the moUiiscan species from one group u[) intcj the next above. Not oidy were these three groups, aggregating more than a mile in thickness, evidently produced by uninterrupted seilimentation, but it seems equally evident that it was likewise uninterrupted between the Laramie and Wasatch epochs, although there was then a change from brackish to fresh waters, and a consequent change of all the species of invertebrates then inlial)iling those waters. Th(^ Wasatch Group, for v/hich •' Vermilion Creek Group" and "I/itter Creek Group" are uncalled for synonyms, in the Green river region, consists very largely of . ;; variegated bad-land sandstones, that reach a thickness of r H)ut 1,5' << feet, together with from 100 to ;}00 feet of the ordinaiy in 'isruLcti sandstones, alternating with bad- land material at the uiise, a, id a siii. xr amount of similar material at top, the estimated ag-' .'^•'*'? i" ''.•' 'less being about 2,000 feet. Kestliig immediately and conformably upon the Wasatch are the strata of the Green River Group. Although intimately connected with the former by continuous sedimentation and specific identity of mol- luscan species, they differ considerably from those of tiuvt group in general as[)ect, and in composition also. The group is lithologically * Am. Jour. Sci. and Arts, 3d sor., vol. xiv. t U. S. Geo. Expl., 40th Parallel. I BuU. U. S. Sur.. vol. iii.. No. 3. f, Wheeler's Sur. W. 100th Mer.. vol. iv. 1 10th Ann. Rep. Hayden's V. S. 'Jeo. Sur Terr. 264 Tertiary. ;h ,it separable into a lower division, having a thickness of about 000 feet, and an upper division liaving a thickness of about 500 feet. Tlie Bridger Group in the t^-pical localities rests conformably upon tiie Green River Group, into which it passes witliout a distinct plane of demarkation among tlie strata. Its molluscan fossil remains corre- spond closel}' with tliose of the Green River Group, some. of the species being tommon to botli, all indicating a purely fresh condition of the waters in wliich the strata of both groups were deposited. In the valley of Red Bluff Wash, between Raven ridge and Wliite river, wiics they are covered by the Brown's Park Group, the thickness is only about 100 feet. The Brown's Park Group is unconformable witli the Bridger Group, but it can not be of later date than Pliocene, for the following i-easons; In many places the strata still remain in a nearly horizontal position, but in others they have been considerabl}' displaced, as, for example, by being flexed up against the flanks of the Uinta mountains, and also, in a similar manner, against the Dry mountains, northeastward from Brown's Park. This shows that, altliough much movement of dis- placement took place before the deposition of the Brown's Pai'k strata, as shown by their unconformity with those of the older groups, a con- siderable amount of movement, even of mountain elevation, has taken place since their deposition, Beside this^ a large proportion of the im- mense denudation which the strata of that region have suffered, is known to have taken place since the deposition and partial displace- ment of the Brown's Park Group, because these strata fire involved with the others in tha't, denudation. Furthermore., a remarkably extensive outflow of basaltic ti-ap, 'lovering a large region whicii lies mainly to the eastward, but which f'ormerl}' extended much within the limits of this district, took place after the deposition of this Group, and also after it had suflfei'ed displacement and erosion to some extent, at least. This is known to be the case, because the trap is found resting upon the unevenly eroded surface of a portion of this group, at Fortification Butte. Tiiat portion occupies a higher level than does the principal poition of the group, and the trap rests unconformably upon the Lara- mie and Gretaceous strata, in the imm>;diate vicinit}-, as well as upon the Brown's Park strata, in such a manner as to show that little, if any, movement has taken place since the trap outflow. The denudation of tlie rocks of that region has been so great since the trap outflow, that the latter rock has been rcnioveil from a large part of the surface it once occupied, leaving only here and there mere shreds of the once mas- sive and extensive sheet upon the higher hills. Memzoio and Ccnnozoic Geology and PaUeontolouy. 265 The Brown's Park Group occupies that expansion of Green rivtr valley wliich is known as Brown's Park. From tlu^re it extends east- ward and around the eastern end of the Uinta uplift, except a few miles interruption of its continuity there, and tlience extends westward along the southern base of the Uinta mountains a large part of the length of that range. It extenls northwai'd from the eastei'n portion of the Uinta mountains, as far as Dry mf)untains and Godiva ridge. Remaining patches of it show that tlie formation formerly extended eastward as far as the foot hills of the Park range. It occupies nearly tlie whole surface of the western portion of Axial basin, comparatively small areas immediately east and immediately north of Yampa moun- tain, and a considerable portion o^t'ie space between Junction moun- tain and the eastern end of the Uinta uplift, all c" which spaces are in unbroken continuity. It, also, occui)ies a large space from Raven ridge and Red Bluff Wash extending far westward. F. M. Endlich observed the Wasatch and Green River Groups spread over an area in the White river region of western Colorado, of more than 3,000 square miles. A section on Douglas creek, a branch of White river, showed a tliicknesss of 1,500 feet for the Wasatch Group. A'stratum of brick-red sandstone, 160 feet in thickness, and placed immediately below the middlo of the Group, served as a land- mark for identification. Inferior beds of coal occur in the upper part of the Group. Groups of columnar monuments, and monuments composed of shales with cappings of sandstones are not uncommon. Fine exposures of the Green River Group occur in the Book Cliffs, Just nortli of the Grand river. Geognostically and lithologically speaking, it is separable into an upper and lower division. The lower arenaceous division having a thickness of 2,400 feet, as obtained from the southern bold escarpment of the plateau, and corroborated by observations elsewhere ; and succeeded by laminated shales, having a thickness of 1,000 to 1,200 feet ; the up[)cr division consisting of yellow and brown sandstones, with thin interstrata of dark shales, and having a thickness of 1,100 to 1,200 feet. These snndstcnc-*, by ero- sion and weathering, have assumed many fantastic s'-ipes. some imi- tating the ruins of some ancient building, and others rising in spires for several hundred feet above their gently sloping surroundings. A group of three of these weathered monuments near Asj)halt Wash, in White rivei- valley, one of which is 80 feet liigh, received the name of the '* Happy Family." On the White river drainage he oliserved no evidence pointing to the 266 Tertiary. h former existence of sjlaciers. The numerous canons cut throusfh the soft shales, marls, and sandstones, are formed so regularly, and {jgree so thoroughly with the pronounced stratigraphical conditions, that they admit of no other agency having shaped them than water. Ascending any one of them toward tiie main divide, the upward slope is found very even, its valley widening wherever other creeks or streams enter, and its entire character in conformity with the view regarding it as the i-esult of the action of flowing water. Dr. A. C. Peale mude a section of the Roan cliffs, at White Moun- tain, on Grand river, where he found the thickness of the Wasatch Group, measured by angles taken with the gradieuter, to be 1,650 feet, and the Green River Group, 2,2S2 feet. George M. Dawson* referred the lignite and basaltic series in the l)asins of the Blackwater, Salmon, and Nechacco rivers, and on Fi'an- cois lake, in British Columbia, to one group, which, on the evidence of the fossil plants, corresponds with the Miocene of Alaska and Gi'een- land. The basaltic and other igneous flows form the latter part of tlie group, but blend with the underlying sedimentary beds, and form an integral part of the whole. No trace, however, is found of rocks due to volcanic action since the period of the drift. The sources of the immense flows of molten matter have been numerous ; for, beside the many dykes found traversing the older rocks, whicli may, at one time, have been fissures giving exit to lava streams, beds characterized by a roughly brecciated character appear in many places, and can scarce- ly have been formed far from the mouths of larger or smaller vents, capable of ejecting fragments. Between the region of the upper waters of the Blackwater and Salmon rivers, and the Bella Coola, three masses of broken mountains represent as many centers of former very great volcanic activity. Samuel H. Scuddev described, from the Tertiary at Quesnel, British Columbia, Sciarn fleperdifa, Euschistus antiqnns. Lachnus quesneli, Bothromicrnmus Inchlanf, and Aranea colnmbioe. The striae upon the rocks of New Hampshirof are extremely variable in their course. A few extremes aro as follows : S. 2° E. ; S. 83° E. ; S. 58° W. ; N. 40° W. ; N. 83° E. Bible hill, in Claremont. rises about 350 feet above the plain of the village, at its northern bast-. What is supposed to be the normal direc- tion of the strijie is abou S. L2" W., which occurs commonly west of * i 1 * i % wi ,i 5' 274 Terlinnj. itt'd part of Canada to the south. The t-ourse of the strije iu sixty si\ UK'alitios between Sherrick's iMount an-.l (Jape Durt'erin vary from S. 45° W. to N. :]5* W., nmny of them a-e S. 60,° 70,° or 80° W., wliile an equal number are N. 00,° 70," or 80' W, The bowlder clays abound with marine siiells. He found abun(Uint evidence that the sea level is falling' at a comparatively rapid rate in Hudson's bay. On the ishuuls and shoi'es all along the Eastmain coast the raised beaches are very conspicuous at all heights up to about thr<;e hundred feet, immc'diately near the sea, but, no (hxibt, higher ones will be fjund further inland. Driftwood (mostly si)ruce) is found almost everywhere, above the highest tides, in a moi'e and more decayed state the higher above the sea, up to a height of at least thirty feet, and in some places up to forty and fifty feet, above wliich it has disappeared by the long ex- posure to the weather. Judging b}' the rate of decay of spruce-wood in this climate its preservation in large (piantities, during an elevation of the land, or ratL:'r a fall in the water, to the extent of thirty' feet, would indicate a change in the relative level of the sea, amounting to perhaps between five and ten feet in a century. The striic observed at eleven places on the east shore of Lake Win- nipeg vary from S. 15° W to S. 45° W. ; at thirty-four places along the boat route from Lake Winnipeg to Hudson's bay, they var^' from S. 50° W. to S. 20° E. ; and at twenty -one places along the Nelson river, from Great Playgreen lake downward, tliey vary from S. 25° W. to S. 80° W. The bearings refer to the magnetic meridian. G. F. Mathew found the course of the grooves and scratches on the rocks in the southern counties of New Brunswick having both south- easterly and southwesterly bearings. A southeasterly course is most prevalent iu the western part of Charlotte county, and a southwesterly course most prevalent in the valleys east and northeast of St. John. These two general courses, as well as the intermediate ones, are con- trolled b}' the contour of the surface of the laud in the several districts where they occur; for, as a general rule, the furrows conform to the di- rection of the river vallevs, or at least are intlueuced in their course bv these depressions. Prof. E. D. Cope* described, from the Truckee beds of the White River Group of Oregon, Ilesperoviys nematodon, iSciurus vortmani, Paciculus insoUtus, Cants lemur, Amphicijon entoptychi, Archmlurux dehilis, Iloplophoneus platycopis, Chamohyus decedens, Thinohyus tri- chobnus, Palaiochcerus aaboiquans, Jlerycojyater guiotianus, Coloreo- * Proc. Am. Phil. Soc I v[: Mesozoi'c (tnd CiKnozoic Oeoloyi/ and Pald-onfoloyy. 27r. don ferox, and C. macrocejihnlu.s; EnhydrorAjon stenncephahts,* K. hasilntusy now Ilymnocyon Ixtnilatvn, Pvehrotherium stcrnbcrgi, Jiooch- (Bras humerosus; and from tho Loup Fork CJroup of Cottonwood creek. Oregon, Lutrictis lycopotamlcus, and Protolabis trnmmontanus; from the Green river shales of Wyoming,! Xiphofryyon acutidens; from the White river beds of Colorado, Auchlsudon tnhifer; and from the Post Pliocene of Shasta county, California, Arctolherium simu)ti, Samuel H. Scuddei^J described, from the thinly bedded, almost paper-like, yellow, gray siliceous Tertiary shales, on the North Fork of the Similkameen river, three miles from its mouth, Penlhetria sim ilkameena, Hygrotrechns stall, Cercopis selwyni, Planop/ilebia yigon- tea, Ccblidia Columbiana; from Nine mile creek, which flov/s into Whip- saw creek, a tributary of the Similkameen, Trox oastaleti, Gallerucella picea, Tenebrio primiijenins; and from the Nicola river, Kebria paleo- melas, Cercyou ( ?) terrigena, liuprestis tertiaria, B. sepu/ta, and Cryptohypnus (?) terrestris. Prof. J. W. Dawson described, from Nine-mile creek, Equisetum sim- ilkamense. In 1880, Prof. E. D. Cope§ described, from the Truckee Miocene of the John Day river, Central Oregon, Nimramis confertus, N. govipho- dus, Pogonodon brachyops; P. platycopis, Hoplophoneus cerebralis, H, strigidens, Dinictis cy clops; from the Loup Fork Group of Ne- braska, Peraceras superciliosus; and from a cave on the Schuylkill river, in Pa., of Post-pliocere age, Smilodon gracilis. Dr. C. A. White|| desci^bed, from the Wasatch Group, near the head of Soldier's Fork, Utah, Planorbis militaris; from the Green River Group, on Henry's Fork of Green river, Wyoming, Planorbis oiqualis, and from three miles east of Table Rock Railroad station, Limncea minuscida; and from the Upper Green River Group of Henry's Fork. Wyoming,^ Pupa atavuncula. Angelo Keilprin** described, from the Eocene of Clarke county, Ala- bama, Cytherea niittalliopsis, Pseudoliva scalina, Lcevibucciniim lineatum, Fnsus subtenuis, F. interstriatus, F. engonat'us, F. sub- ',|!,K * Bull. U. S. Geo. Sur. Terr., vol. v. •r Am. Nat., vol. xiii. I Geo. Sur. of Canada. ^ Am. Nat., vol. xiv. II Proc. U. S. Nat. Mus. 1[ 12th Rep. U. S. Geo. Sur. Terr. '•■• Proc. Acad. Nat. Sei. ■? t IMAGE EVALUATION TEST TARGET (MT-3) // .< ,.v '^ ^^< i Ss 1.0 1.1 11.25 1^128 |2.5 |iO ■^" M^H us Kii 12.2 ui Hi us i; UiL 12.0 ■UUU. 1.4 IIIIII.6 Photographic Sciences Corporation tony fragments or pebbles, and less cal careons and more aluminous matter than the blue hard pan. It is not quite as solid as the blue, more pervious to water, and contains more and larger pieces of primitive rocks. The clays of the country, used for bricks are principally of this bed. It forms a hard, stiff soil, adapted for grass. The flat regions and savannas of the northwest quarter of the State, are caused by the surface presence of this bed. 3d. "Sand and gravel drift," containing granite bowlders (in small numbers), of large size, and unconformable to Nos. 1 and 2, and the other rocks. It exhibits little regularity of stratification, is composed of inferior patches of coarse sand and gravel, intermingled at all in- clinations, evidently the result of long continued and vigorous action of watt" in rapid motion. The gravel is coarse, but much worn, rounded and smooth, like the gravel beds of rapid streams. The por- tion of earthy matter is about one half, of a reddish and yellowish col- or, showing the presence of oxide of iron, and containing various pro- portions of sand and clay. Almost every rock in the northern part of America is represented in the gravel; but the greatest part by far is from the underlying and adjacent strata. There are pebbles of quartz, trap, granite, gneiss, conglomerate, limestones of all ages, iron ore, slate, coal and sandstone. In this there has been found timber but very rarel3% 4th. The " valley drift," composed principally of debris of the ad- jacent rocks, and occupying the lower parts of the great valleys of drain- age. It is more gravelly and less earthy, and the gravel is more of local origin tlian in No. 3, while the beds of sand are less common. It is in the " valle}-^ drift'' or swamp mud that the bones of the mastodon and other large animals are usually found. :t!ii 208 Tertiary. il 4 IB ■f' ■ s I' : i ' Hi ; ■ 't 1 i'i t - 5tli. " LaciiHtrinc deposits," occupying tlie basin of tho lakes, and for Lake Erie, divided into the " blue marly sand," and the coarse sand and gravel. The " blue niaily sand," coinmoiily called the blue clay of Lake P^rie, is seen skirting the >ihore almost everywhere, if the coast is not rocky, — its upper face nearly horizontal, and rising from forty-five to sixty feet above the water. Tt is of a light blue color, so fine as scarcely to show between the fingers any grit, homogeneous, and in a dr\' static compact, bu^ brittle. Very rarely, may be seen a primitive pebble, thin layers of leaves and lignite. Tt is distinctly and horizon- tally laminated, and at Cleveland is cotnposed of about 75 per cent, im- palpable sand, 3 per cent, iron, fi to 7 per cent, carbonate of lime, 9 per cent, carbonate of magnesia, and of vegetable matter and sulphur. Tt is impervious to water, and thus causes thousands of springs to ap- pear at its surface, which, passing out over the edges, dissolve and carry it away verj' fast, forming a quick sand. Tts edge is pre«iented to the action of the waves, which dissolve and carry it away rapidly. As it is not tenacious like cla}', and not capable of sustaining itself under its own weight, and that of the sand stratum that rests ui)on it, there are continual breaks and slides along the banks, on both the American and Canadian shores. These avalanches of earth arc from one to four rods in width, breaking off in irregular patches, and some- times sinking, in a night or in a few hours, twent}' or thirty feet, leav- ing huge fissures through which the water of the springs passes, and rapidly washes the earth into the lake. At the water's edge, the slide frequently raises a bank of about the width of the break, several feet above the surface, driving back for a short time the line of the shore. But the waves acting incessantly dissolve the new barrier, and soon commence their attacks upon the body of the fallen mass, which disappears, and is before long followed by a fresh avalanche from above. At the city of Cleveland, where the bluff shore rises 70 feet above the lake, the encroachment since the survey of the town in 1796, has been at tho foot of Ontario street, 265 feet. The Canadian shore, from Detroit river to Long point, is losing faster than the American. Be- tween Port Stanley and Port Rurwell, on the British side, the superior face of the blue marl is about sixty feet, or fifteen feet higher than at Cleveland, and has in the upper part a lighter or more yellow color. In composition the yellowish portion is more argillaceous than the bright blue, and appears to correspond with the yellow clay stratum of Lake Champlain. The gi-eatesL thickness of the blue murls can not be com- V. t' ■■i il McHozoic niul Cn-noznic Genhujif and J*ala>onf()Jof/tf. 20!) [)ute(l, as 11 largo part of it lies below the lakn level, formiiii:; the hod of more than one half of Lake Erie. On the south shore it extends hut a short distance into the interior, forming a narrow belt of low eountry along the lake, and thinning out as the roeks upon whieh it rests rise to the southward. •The *' coarse sand and gravel" of this division, rests conformably on tho " blue marly sand," and spreads horizontally over a tract of low, and in general wet land, embracing the western half of Tiake Krie, and extending westward into the States of Ohio and Michigan. On the north, it forms the soil and surface ovct a large portion of tin; peninsula, between Lakes Krie and Huron; whieh seldom rise more than 200 feet above the waters of these lakes. On it, and composed of its coarse water washed sand and gravel, are seen the "lake ridges," objects of curiosity, and of much utility in a new country, being nat- ural turn[)ike8 that run parallel with the shore. At Cleveland the section is as follows: 1st. Gray, water-washed, coarse sau'', resting on the blue marl, 10 feet. 2d. Coarse gravel of the adjacent rocks and sand, 20 to 40 feet. The lake ridges are not precisely horizontal, and are found atvarions elevations, W, 90, 120 and 140 feet above the water. There are branches and cross ridges uniting different pf.ra'lels, that rise and fall several feet in a mile. 6th. Bowlders or "erratic rocks" which he regarded as a ''stratum," and the newest of all l)eds except the alluviunj. The Drift deposits* are very extensive on the southern shore of Lake Superior, and more especially on its southeastern coast. There they not only constitute the only visible formations for nearly 100 miles, but they also attain an astonishing thickness, so as to form, by themselves, ridges and cliffs which exceed in height even those of the Pictured Rocks, being in some places, as at the Grand Sable, not less than 360 feet high. The Drift is less conspicuous along the western portion of the lake shore, although it is not wanting even among the romantic and precipitous cliffs of the Pictured Rocks and the Red Castles. The Drift of lake Superior may be divided in ascending order, into — 1st. Coarse drift. This is the least conspicuous of all. It is found only in a few places along the southern shore, generally capping the high towering cliffs of sandstone. It is generally a mixture of loam and fragments of rock of different sizes — sometimes worn, but more generally angular. As a leading feature, it is almost exclusively com- * Foster and Whitney's Sur. Lake Sup. Region, 18.50. .'{00 Tertlnrii. if I » i: ,1 la n IK poHOfl of frajrmcnts of tho rocks in situ, Hhowiiijr ilmt, whntevnr mny liiivn l)oon its origin, it could not have been acted upon by long con tinned agencies. A few foreign pebbles exist in if, genernlly trap, and evidently derived from the nund along the whole southern coast of lake Superior, resting upon the red sandstone, and limited to a certain height, but on tho Ontonagon and Carp rivers, it is found in depressions ;m elevated lands, 500 feet above the lake. At Grand Sable wliore its base rests on almost horizontal strata of red sandstone, a few feet above tho water, and its top is covered by a mass of drift sand, it is 60 feet in thickness, and ex hibits lines of stratification disposed with great regularity. 3d. Drift sand and gravel. This is the most widely diffused of the drift deposits on the shores of lake Superior and the northern part of Michigan. The greatest thickness observed is at Grand Sable, where it is 300 feet thick. 4th. Bowlders. These occur of every size and description in great numbers along the whole southern shore. The largest noticed being of hornblende, and measuring 15 feet in length, 11 in width, and 6^ in height. The bowlders have been moved from north to south, but have not come from far, though some of them have been transported from the north shore. It is noticed among the ridges north of Carp river, that the valleys, for the most part, contain bowlders from the next ridge to the north; and there are instances where a ridge did notallo^\ the fragments of the preceding ridge to pass. This limitation pre- vails only within the hilly portion of the Lake Superior region between the lake shore and the dividing ridge. South of this ridge no barrier occurs. 5th. Drift terraces and ridges. These may be seen both on the north and the south sides of Lake Superior, but the}' are less striking than around Lakes Erie and Ontario. The}' are most conspicuous on the south shore, between Saut and Keweenaw point. Their average lieight is about 100 feet. At a place two miles east of Two hearted river, the following succession occurs : gravel beach, 5 feet ; sand i; i ': :' ■ 1 . 1 * 1 ' Mmozoh' find Cnnozoir Geology and PnlcBonfolotjy. 'M\l beach, 12 foet ; l»l drift ternuund instrumonti and also wide bowl-i^haped depressions, known as troughs, which have been caused by the same agenuy. Grooves and scratches were ob- served on the road from Eagle river to the Clitt' mines running N. 15° E. On an island oast of Dead river there are two systems of striie — one running N. and 8., and the other N. 20° E. and S. 20° W. The rock here which is very hard and tough hornblende, isnotonl^ groovetl and furrowed over its whole extent, but there are, beside, deep trough like depressions, with perfectly smoothed walls, some 12 to 15 feet long, 4 feet wide, and 2| feet deep. On Middle Island, east of Granite- point, troughs may also be seen 4 feet wide, and 2 feet tieep, running like the stria3 N. 20'' PI On the promontories and islands near Wor- cester, two miles west of the mouth of Carp river, there are two distinct sets of 8tri>e ; those running N. 55° E. are the most numerous ; those running N. 5° E. the least. The latter cross the former and are there fore more recent. Some of them are, beside, distinctly curved, as if the body which produced them had been deflected in ascending the slope. Each set of striai extends only about one foot below the water's edge. On the first quartz ridge, one mile from the mouth of Carp river 500 feet high, the striaj run N. 20° E. On the iron ridge south of Teal lake, 750 feet high, the strioe run N. 55° E. At the Jackson forge N. 65° E. A green magnesian rock, with vertical walls, and semi- cylindrical form, on the road leading from Jackson landing to Teal lake is covered with strite which may be traced along the surface, like hoops around a gigantic cask. On Isle Royal the strire run N. 50° E. with many local deviations. On the shores of Ackley bay striaj near the water's edge running E. and W., cross others running N. E. and S. W., and i/thers again running S. 75° E. Isle Royale presents but little evidence of drift, though scattered bowlders are found upon it; the surface of the rock s are generally, however, smoothed, as if polished off. Mr. E. Desor described the superficial deposits on the northern shore of Lake Michigan, the western shore of Green bay, the Big Hay ] i:o,ii: ■h ynii . 302 Tertiary. (les Noquets, and the valleys of the Menomonee and Manistee. The coarse drift described as occurring beneath the drift proper, at several jjoints along the shore of Lake Superior, seems to be entirely wanting in this district. Starting from Mackinac westward, the furrows and strise were noticed at the bottom of St. Martins ba}', and two miles north of Pine river, on a point composed of almost horizontal ledges of limestone, having an average direction fi'om E. to W., some running N. 80° E., and others S. 70° and 80° E, At Payment point the direction being from N. 50° to N. 60° E. At the bottom of Big Bay des Noquets, on the west shore of the eastern cove, the direction is E. and W. At the mouth of the Escanaba, in Little Bay des Noquets, the direction is N. E. and S. W. At Oak Orchard, on the west shore of Green bay, the direction is N. 15° to N. 20° E. At the saw mill, near the mouth of the Menomonee, the direction is K. and W. ; six miles above Kitson's trading house, E. N. E. and W. S. W. ; three miles above Sturgeon's falls, N. 65° E.; foot of the Lower Bukuenesec falls, N. 70° E.; Lower Twin falls, N. G0° to N. 70° E.; and at Upper Twin falls, N. 65° to 70° E. From Green bay, southw^estward, the}' were noticed at INlehoggan point, N. E. by E. and N. N. E. ; at Mehoggan falls, N. E. by N. ; three miles west of Milwaukee, N. E.; and at Strong's landing on Fox river, N. E. by E. The true drift seldom approaches the shores of Lake Michigan and Green bay, but it is mei with in ascending the rivers at no great dis- tance. Its absence from the coast is the result of subsequent denuda- tion, when the waters of the lake stood at a higher level than at present. It was observed at Poiute aux Chenes, and for a distance of six miles toward Payment point, and on Potawatomee and some of the highei- islands. The thickness at Green ba}' was found on boring to be 108 feet. Near the junction of the Machigamig and Brule, where the united streams take the name of Menomonee, the river banks are composed of drift, forming bluffs 100 feet or more in height. The drift is com- posed of sand and layers of gravel more or less interspersed through it, and covered more or less with bowlders. The higher lands adjoining are covered with the same materials. The country adjacent to the Manistee is likewise covered with the drift sand and pebbles. The whole country drained by the White-fish and its branches, and the Escanaba is likewise covered with the drift. The drift clay is well marked, in many places, below the drift sand, especially upon the Mesozoic and Ccunozoic Geology and Paleontology. 3o:i %{) Manistee, where it does not generally reach more than 4 or 5 feet above the river, although in one place it was found 10 feet thick. It is very tough, and generally' flesh colored, but in oue instance it was perfectly whitt^. There were observed, in several localities, rather coarse pebbles of limestone, and even flat stones intermixed with the upper layer of clay, near its contact with the sand. He described the terraces on the island of Mackinac and the neigh- boring coasts, on the west coast, and at Pointe St. Ignace and Gros Cap on the north coast of Lake Michigan, which vary in height from 20 to 130 feet. But the terraces are not found farther west on the north shore of Lake Michigan and Green bay, nor in the vicinity of the Menomonee and Manistee. Mr. Charles Whittlesey,* said of the terraces bordering Lake Erie, that the first ridge, or that nearest the lake, is known as the '• North ridge." From Conneaut, in Ashtabula count}^ to Russelton, Huron county, a distance of 120 miles, the elevation of the ridge above the lake varies from 85 to 145 feet. The second ridge, from Kingsville, in Ashtabula count}', to Ridgeville, in Lorain count}', varies from 122 to 168 feet above the lake. These ridges consist of coarse, water-washed, yellowish sand, or of fine gravel, principally' the comminuted portions of the adjacent rocks. The rocky fragments are not generally worn per- fectly round, or oblong, as beach shingle is, but are more flat, with worn edges. There are mingled with the sandstones and shales that compose this gravel, scattered pieces of quartz, flint, granite, trappean rocks, limestone and ironstone. The third and fourth ridges are a little higher, and composed of coarser material. In 1852, Charles Whittleseyf described the drift in that part of Wis- consin bordering on Lake Superior, and lying between the Michigan boundary' and the Brule river, and the sources of tiie streams flowing into Lake Superior from the south. He divided the drift into — 1st, red marly clay; 2d, bowlder drift, coarse sand and gravel. The red marly clay is a fine-grained, homogeneous marly sand, cemented b}^ argil or cla}', with well defined horizontal lines of laminn- tion or deposition; containing, but ver^' rarely, pebbles of granitoid, trappose, sandstone, conglomerate, or slate rocks. This constitutes the shore or lake bluffs most part of the way from the Montreal to the Brule; the red sandstone, on which it rests, showing itself occasionally beneath. It is easily washed away in suspension by tlie waves, and * Am. Jour. Sei. and Arts, 2d ser., vol. x. t Owen's Geo. Sur., Wis., Iowa, and Minn. 304 Tertiary. liavin<5 little tenacit}', falls in slides and avalanches into the water, and is thui' cut into deep, narrow j^ulliesby rains. Its surface in the above district is not more than 250 feet above the lake, sloping gradually from the mountains to the shore, as though it formed, at one time, the bed of an ancient sea. On the waters of the St. Louis river on the west, and the Ontonagon on the east, however, the red clay deposits reach to the height of 450 to 500 feet above the lake. On the " Isle aux Barques" the lime is so abundant in the clay, that it has formed in amorphous concretions throughout the mass. A few lea/es and decayed sticks have been seen in the red marl}' clays, with carbonaceous matter and lignite, but such occurrences are rare. Along the coast there are interstratified beds of sand and gravel of a local character. In the interior, where the clay is visible in bold bluffs, along the water courses, it is more uniform and less inter- calated with coarse drift. It rests not only on the sedimentary unaltered rocks, but also on trap and metamorphic and igneous rocks. The mass of the hills between Chegwomigon bay and the Brule river, is gravel and bowlder drift. It is not very uniform in composition, and is marked by the violent action of water. The central part of this peninsula presents large tracts of barren, water- washed land, and mod- erately coarse gravel. Both the western and eastern knobs and ridges are of coarse materials; and toward the point or extremity about the "detour," and the adjacent islands, the sand and bowlder deposits are represented. A section of three miles from the coast to the mountnins, four miles southwest of LaPointe, showed red marly claj' 95 to 130 feet above the lake, capped by coarse bowlder drift, the top of whicli is 428 to 509 feet above the lake. This drift is disposed in three very abrupt and well defined terraces. These terraces continue southward around the southern extremity of the mountain, and have the appearance of ancient beaches or shores. In 1855, Prof. G. C. Swallow* found a fine, pulverulent, absolutely stratified mass of light, grayish bufi", silicious and slightly indurated marl, capping nearly all the bluffs of the Missouri and Mississippi within that State, for which he proposed the name Bluff lormation. The Bluff above St. Joseph exhibits an exposure 140 feet thick. It is easily penetrated by the roots of trees, which decay and leave en- crusting tubes, giving it a peculiar perforated appearance. It extends from Council Bluffs to St. Louis, and below to the mouth of the Ohio. * (leo. Sur. of Missouri. Jlenozoic and Ccenozoic Geology and Pahuontoloyy. 305 The greatest development is in the counties on the Missouri, from the Iowa line to Boonvillc. In some places it is 200 feet thick. At Boon- ville it is 100 feet thick, and at St. Louis only 50 feet. The Bluff' Group is older than the bott(.m prairie, and newer than the Drift. It gives character and beauty to nearly all the best landscapes of the Lower Missouri. He found the drift abounding north of the Missouri river, and ex- isting in small quantities as far south as the Osage and Meramec. Its thickness varies from 1 to 45 feet. The upper part, having the ap- pearance of having been removed and rearranged by aqueous agencies since its first deposit, but before the deposit of the Bluff Group, is described as altered drift. The heterogeneous strata of sand, gravel, and bowlders, is called the bowlder formation; and below this, in some places, a third division exists, which is called the "pipe clay." It contains bowlders more or less dispersed through the upper part of it. It is found in Marion, Boone, Cooper, Moniteau, Howard and Monroe counties, varying in thickness from 1 to G feet. William P. Blake* described the grooving and polishing of hard rocks and minerals by dry sand in the Pass of San Bernardino, Cali- fornia, and on the projecting spurs of San Gorgonia. he said, grains of sand were pouring over the rocks in counties:^ myriads, under the in- fluence of the powerful current of air which seems to sweep constantly through this Pass from tlie ocean to the interior. Wherever he turned his eyes — on the horizontal tables of rock, or on the vertical faces turned to the wind — the effects of the sand were visible; there was not a point untouched, the grains had engraved their track on every stone. Even quartz was cut away and polished; garnets and tourmaline were also cut and left with polished surfaces. Masses of limestone looked as if they had been partly dissolved, and resembled specimens of rock salt that have been allowed to deliquesce in moist air. These minerals were unequally abraded, and in the order of their hardness; the wear upon the feldspar of the granite being the most rapid, and the garnets being affected least, wherever a garnet or a lump of quartz was im- bedded in compact feldspa:, and favorably presented to the action of the sand, the feldspar was cut away around the hard mineral, which was thus left standing in relief above the general surlace. A portion however, of the feldspar, on the lee side of the garnets, being protected from the action of the sand by the superior hardness of the gem, also stood out in relief, forming an elevated string, osar like, under their 'I'M Am. Jour. Sei. and Arts, 2d sor., vol. xx. 306 Tertiary. in A 1 lee. When the surface acted on, was vertical and charged with gar- nets, a very peculiar result was produced; the garnets were left stand- ing in relief, mounted on the end of a long pedicle of feldspar, which had been protected from action while the surrounding parts were cut away. These little needles of feldspar tipped with garnets, stood out from the body of the rock in horizontal lines, pointing like jeweled fingers in the direction of the prevailing wind. The effects of driven sand are not confined to the pass; the}' may be seen on all parts of the desert where there are any hard rocks or minerals to be acted upon. On the upper plain, north of the Sand Hills, where steady and high winds prevail, and the surface is paved with pebbles of various colors, the latter are all polished to such a de- gree that the}' glisten in the sun's rays, and seem to be formed b}' art. The polish is not like that produced by the lapidary, but looks more like laquered ware, or as if the pebbles had been oiled and varnished. On the lower parts of the desert, or wherever there is a specimen of silicified wood, the sand has registered its action. It seems to have been ceaselessly at work, and when no obstacle was encountered on which wear and abrasion could be effected, the grains have acted on each other, and by constantly coming in contact have worn away all their little asperities and become almost perfect spheres. This form is evident whenever the sand is examined by a microscope. We may regard these results as most interesting examples of the denuding power of loose materials transported by currents in a fluid. If we can have a distinct abrasion and linear grooving of the hardest rocks and minerals, by the- mere action of little grains of sand, falling in constant succession, and bounding along on t'»eir surface, what may we not expect from the action of pebbles and bowlders of great size and weight, transported by a constant current in the more dense fluid, water? We ma}' conclude that long rectilinear furrows of indefinite depth may be made by loose materials, and that it is not essential to their formation that the rocks and gravel, acting as chisels or gravers, should be pressed down by violence, or imbedded in ice, or moved forward en masse under pressure by the action of glaciers or stranded icebergs. Wherever, therefore, we find on the surface of moun- tains, not covered by glaciers, grooved and polished surfaces with the furrows extending in long parallel lines seeming to indicate the ac- tion of a former glacier, we should remember the effects which may be produced during a long period of time by light and loose materials transported in a current of air; and which, consequently, may be pro- Mesozoic and Cmnozoic Geology and Pabvontolor/y. :{07 duced with greater distinctness, and in a dilTerent style, by rocks moved forward in a current of water. The effects produced by glaciers, by drift, or moving sand, are doubtless different and peculiar, so dif- ferent and characteristic, that the cause may be at once assigned by the experienced observer, who can distinguish between them without difficulty. It is, however, possible that after a sand worn surfnce, such as has been described, has been for ages covered with moist earth, a decomposition of the surface would take place sufllciont to remove the polish from the furrows and leave us in doubt as to their origin. Alexander -Murray* examined a portion of the country between Georgian bay in Lake Huron, and the Ottawa river. He followed the course of the Muskoka river to its head, and by a short portage passed to the source of the Petewahweh, and by its channel de- scended to the Ottawa. Returning, he ascended the Bonnechere river to Round lake, from which he crossed to Lake Kamaniskiak on the main branch of the 3Iadawaska, and descended the latter stream to the York or southwest branch, from whence he crossed to lialsam lake. He found stratified clays on the Muskoka, between the lake of Ba3's and Ox-tongue lake, at the height of about 1,200 feet above the level of the sea; tiie banks expose 10 or 12 feet in thickness, of drab or lij^ht buff-colored clays, alternating with very thin layers of fine yellow or grayish sand. At one place, the beds are tilted, showing a westerly dip of about eight degrees, in which they cxlMbit slight wrinkles or corrugations. Coarse yellow sand overlies the clay, and spread'j far and wide over the more level parts, generally forming the bank of the river, where not occupied by hard rock. On the Petewahweh, especially below Cedar lake, the whole of the level parts are covered with sand, which, in some places, is of great thickness. Cedar lake is about 1,050 feet above the sea. The banks of the Bonnechere display a great accumulation of clay at many parts below the fourth chute, sometimes exposing a vertical thickness of from 70 to 80 feet. Near the mouth of that river, below the first chute, where the clays form the right bank, and are u inward of 50 feet high, they are chiefly of a pale bluish-drab color, and are calcareous, while other clays found higher up the stream, are of a yellowish-buff, and do not effervesce with acids. Below the second chute, buflT-colored clay is interstratified with beds of sand and gravel, the latter sometimes strongly- cemented together by carbonate of lime, the whole being overlaid by a deposit of sand. The gravel is seldom ii IIP Geo. Siir. of Can., Rep. of Progr. for Ifi'ilJ. :jo8 Tertiary. 1: l%| very coarse, although an individual bowlder may occur here and there amongst it, and it is chiefly derived from tlie rocks of the Laurenlian series. The height of the first chute above the sea, is 2(55 feet; the second chute, 348 feet; the fourth chute, including its fall of 39 feet, 432 feet; Round lake, r)20 feet, or nearly GO feet below Lake Huron. Sand is extensively distributed over the plains of the Bonnechere, and over a large portion of the area between it and the valley of the Madawaska. Most of the valley of the Little Madawaska is covered with sand on either side, and the country' between its head waters and Lake Kamaniskiak is one continuous sandy plain. The height of land in passing over the portage to the Madawaska is 9G8 feet abuve the sea, and Lake Kamaniskiak is 006 feet above the level of the sea. No organic remains have been detected in any of these drift deposits. He, afterward,* surveyed the valley of the Mcganatawan river and part of the coast or Lake Nipissing. Stratified ela}^ was found on the banks of the Meganatwan, abov3 the second long rapids, east of Doe lake. The color is a brownish drab; it is very tenacious, and does not effervesce with acids. The highest exposure is a little over 1,000 feet above the level of the sea. A fine, strongly tenacious cla}' occurs on the Nahmanitigong near the main elbow, where the upward course of the river turns to the south at an elevation of 710 feet above the sea. The color of the clay is chiefl}' pale drab or buff, but bands of reddish clay are interstratified and some of pale blue overlie the whole. The clays of the interior are usually overlaid by a deposit of coarse yellow sand. Among the bowlders on Lake Nipissing, man}' were observed to be of a slate conglomerate like that of the Huronian series, and they were frequently of very great size. In the succeeding 3'earf he explored portions of the Huron and wes- tern districts of the Province of Canada, and found that the course of the currents which had borne along tl)ontolr>riy. 311 envelope detafhed partu'le.s of saiul, Hinall pebbles ami aji^gregations of particles of sand. Above the fine stratilied elay, yellow clay aud un- stratilied sand occur. Bowlders are found on the Qn'Appelle and its allluents, lielow the Moose Woods, and north of the Assiniboiiie, measuring- from 10 to 25 feet or more in diameter. In Lake Winnipeg, ice every year brings vast bowlders and frag- ments of rock of the Laurentiau series, which occupy its eastern shores, and distributes them in the shallows and on the beaches of the western side. In Lake Manitobah, long lines of bowlders are aecumu kiting in shallows and forming extensive reefs; the same operation is going on in all the lakes of this region, and is instrumental in diminishing the area of the lake in one diro(!tion, which is probably compensated by a wearing awa^' of the coast in other i)laces. A remarkable beach and terrace, showing an anciimt coast line be- tween Lake Superior and Lake Winnipeg, separates Great Dog from Little Dog lake o'l the Kaministiquia canoe loute. The Great Dog- portage, 55 miles from Lake Superior b}- the canoe route, rises 490 feet above the level of the Little Dog lake, and the greatest elevation of the ridge can not be less than 500 feet above it. The difference be- tween the level of Little and Great Dog lakes, is 347.81 feet, and the length of the portage between, one mile and 53 chains. The base of the Great Dog mountain consists of a gnelssoid rock, supporting numerous bowlders and fragments of the same material. A level, plateau of clay then occurs for about a quarter of a mile, at an altitude of 283 feet above Little Dog lake, from which arises, at a very acute angle, an immense bank or ridge of stratified sand, holding small water-worn pebbles. The bank of sand continues to the sum- mit of the portage, or 185 feet above the clay plateau. East of the portage path the summit is 500 feet above Little Dog lake. Here we have a terrace 500 feet above Little Dog lake, oi 863 feet above Lake Superior, or 1,403 feet above the sea. Another beach or terrace occurs at Prairie portage, 104 miles by the canoe route from Lake Superior, 190 feet above Cold Water lake, or 900 feet above Lake Superior, or over 1,500 feet above the sea. In the valley of Lake Winnipeg, the first prominent beach or terrace is the Big ridge. Commencing east of Red river, a few miles from the lake, it pursues a southwesterly course until it approaches Red river. v.ithin four miles of the Middle settlements; here it is 67^ feet above the prairie; on the opposite side of the river, a beach on Stony moun- :U2 Tevtiary. 1 tain corruspoiuls with tlio \\\)X, ri(le, where it has been rcMuoved by the Prairie Portaye river and the waters of the Assiniboine. It may be seen again on White Mud river, about 20 miles west of Lake Manitobah. In the rear of Dauphin lake, the next ridge in ascending order occurs; it forms an excellent pitching track for Indians on the east Hank of the Riding mountain. At Pembina mountain four distinct steps or beaches occur, the summit of which is 210 feet above the prairie. Tlie lower prairies enclosed by the Big Ridge are everywhere inter- sected by small subordinate ridges which often die out, and are evi- dently the remains of shoals formed in the shallow bed of Lake Winni- peg, when its waters were limited by the Big ridge. The long lines of bowlders exposed in two parallel, horizontal rows, about 20 feet apart, in the drift of the south branch of the Saskatchewan above mentioned, are the records of former shallow lakes or seas in that region. They may represent a coast line, but more probably low ridgjs formed under water, upon which bowlders were stranded. The fine layers of stratified mud, easil^y split into thin leaves, which lie just above them, show conclusively that they were deposited in quiet water; their horizontality proves that they occupied an ancient coast or ridge below the comparatively tranquil water of a lake of limited extent; the vast accumulations of sand and clay above them establish the antiquity of the arrangement; and the occurrence of two such layers, ))arallel to one another, and separated bj^ a considerable accunmlation of clay and sand, leads to the inference that the conditions which established the existence of one layer also prevailed during the arrangement of the other. It may be that these are bowlders distributed over the level floor of a former lake or sea, and they msiy cover a vast area. The Pembina mountain is par excellence the ancient beach in the valley of Lake Winnipeg. It is not a mountain, nor yet a hill. It is a Mdsozoir (Did Cmnozoir Genlof/i/ nutf Vnl(jin)ilitln00 and l.()(H) feet above the oecan level. High above lVnd)ina mountain the stens and plateaux of the Riding and Duck mountains ariso in well dellned sue C'essi(ui. On the southern and southwestern slopes of these ranges tiie terraces are distinctly detined, on the northeast and north sides the Riding and Duck mountains present a precipitous (;scarpment which is elevated fully 1,000 feet ai)ovo Lake; Winnipeg, or more than 1,000 feet above the sea. One of the terraces here is I,42(S feet above the level of the ocean. The' denudation of the (Cretaceous, in the valley of Lake Winnipeg, lias been enormous, because tlu^ shales crop out 500 feet above Daui)hin lake, where their position is nearly horizontal, and evincing their former extension to the northeast, if not as far as the north shore of Lake Winnipeg. Sand hills and dunes occur on the Assiniboiiie, Qu'Appelle, South IJranch, and north of Touchwood hills, Prof. Vj. W. Hilgardf described the drift (he called it the Orange Sand formation) as covering the greater part of the State of Missis- sippi. It is overlaid by the lilutf Group, and is not. therefore, above Natchez, exposed o;i the surface, within eight to twelve miles of the Mississippi river ; below Natchez, however, it forms the White cliffs on the Mississippi itself. It does not cover the northeastern part of the State, and is absent from other limited patches. The thickness is quite variable, sometimes reaching 200 feet, though usually not more than 40 to 60 feet. The material is usually silicious sand, colored more or less with hydrated peroxide of iron, or orange- yellow ochre. Sometimes pebbles or shingle, either cemented into puddingstone, or more frequently loose and commingled with sand or clay occur, and at other times limited deposits of clay are found. It contains fossils from the Silurian, Devonian, Carboniferous, and Cre taceous formations which are exposed to the north in Tennessee, Ken- tucky, Indiana, Illinois and Ohio, and silicified wood from the lignite strata of Mississippi. The character of the surface upon which it rests its own irregular stratification, and the dependence, to a great extent, of the nature of its materials, upon that of the underlying formations, proves, beyond question, that its deposition, pi-eceded and accompanied bj' extensive denudations, has taken i)la.e in flowing water, the effect of whose weaves, eddies and counter currents, is j)lainl^' recognizable in numerous profiles. Nor can there be any doubt that the general diroc- * Geo. Sur. of Miss. f 1! . ) . : J I i :tl4 Tei'fidt'!/. I tioii of the ciHTiMit was from north to Hoiitli, iiltlionj^h lociilly clmii^fcil (»r (lirt'C'tcd hy the pre existinj;' ■mo(|iiiiliti('s of tb.c surface. The drift is Hiiceccchid on the MiHsiHsippi by si narrow belt, ealled th(! Hluf! Group, but in other parts of tlie State the; drift is eovered by a y(.'llow loam, which also sufeeeds the niulf. The second bottom, or Ilointnoek deposits, and the alluvial, are yet more recent in their char acter. Drift materials"* ar(! strewn over a jjfreat [)art of the surface of Michi '^iiu. At Kast Sa<^inaw these luatei'ials arc from 00 to 100 feet thick, and at Detroit DJO feet thick. Wherever large surfaces of the under- lyiuj^ rocks are exposed, they arc; found to be more or less smoothed and striated. The island of Mackinac shows the most indubitable evi- ilence of th(! former height of the water, 2r)0 feet above the level of the lake. The trunks of white cedar trees are not uncommon in the drift, and on the north shore of Grand Traverse bay there is a bed of lignite. In 18()2, Prof. J. D. Whitney pointed ont,f approximately, the terri- tory in northern Illinois, western Wisconsin, northeastern Iowa, and eastern Minnesota, that is destitute of drift. This tract is several hundred miles in length, and from 100 to 200 miles in width. There is an entire absence of bowlders or pebbles, or any rolled and water- w;)rn materials, which by their nature would indicate that the region in question had been exposed to the action of those causes by which the drift phenomena were produced. The surface of the rock is uneven and irregular, bearing the marks of chemical rather than of meclmnieal erosion, and there are no furrows, stria; or drift scratches, such as may be observed on many of the rocks over which the drift has been moved. He concluded: 1st. That there has existed, ever since the period of the deposition of the Upper Silurian, a considerable area, chiefly in Wisconsin and near the Mississippi river, which has never been sunk below the level of the ocean, or coveivd bj' any extensive and permanent body of water, and which, consequently, has not only not received an}' newer deposit than the Upper Silurian, but has also entirely escaped the in- vasion of the drift, which took place over so vast an extent of the northern hemisphere. 2d. That the extensive denudation, which can be shown to have taken place in this region, as witnessed by the outliers of rock still re- maining, and the general outline of the surface, has not been occasioned '•' Geo. Sur. of Mich.. 1861. T Geo. Sur. of Wisconsin. MeHozoic find Cn-iiozoi<' Geolotji/ nnd /'a/n oiifnloiji/. '.\Uy by any ciirrcMits of wat«'r HWCM'piiijjf ow.v i\n> Hiirfiici', iimlcr soin*' i?i('iit gt'ticrtil ciiiisc, Imt tliiit it litis nil Ix't'ii quietly iiiid siU'iitly ctl't'clt'd by the Hiii)i)I(! tir, there is a deposit of the roots and limbs of trees, im- bedded in a bluish scaly material, apparently a mass of compressed leaves and moss, which rests upon a bed of clay, and is overlaid by a mixture of clay and sand; the whole, with a stratum of sand at the top, constitutes a bank of from 20 to 24 feet high. The bed of vegetable matter, which is from one to three feet thick, and about ten feet over the river at the western end of the exposure, dips gently and evenly up the stream; while a thin bed of reddish clay, intervening between the overl3'ing arenaceous clay, and the stratum of sand which forms the surface, seems to be perfectly horizontal. On the south side of Lake Superior, letween White-fish Point and the Painted Rocks, a great deposit of sand, interstiatified with gravel, is spread over the surface of the country. At the Grand Sable, a short distance west from the Grand Marais, it rises here and there almost vertically from the lake to a height of 300 feet. A bed of vegetable matter occurs below a layer of mixed sand and clay, and beneath this hill of sand and gravel, which contains Thuya occidentalism Betula paperacea, and populus balsarnifera. Behind the Sault Ste Marie, a terrace, varying in its height, but averaging perhaps 150 feet above Lake Superior, and often composed of clay in red and drab layers, stretches from the Laurentide hills southward towo'-"" the St. Mary river. About a mile below, and again about four miles above the foot of the Sault, this terrace comes near Wi Mesozoic and C!:i; •.\u Tertiary. H; In tlio thiee prairie steppes tliere is a marked difference in tlie gen- eral aspect of the surface of the country, and in the character of the river valleys. On the first steppe, the surface 's usually level, or un- dulating in long gentle sweeps, and the beds of the principal streams do not, probably, average more than 30 feet below the level of the sur- rounding country. On the second steppe the surface is rolling, and the river valleys are usually from 150 to 200 feet in depth, while on the third, the hills are on a larger scale, and either closely crowded together, or they rise here and there to considerable heights overlook- ing less rugged tracts. The principal river-valleys on this steppe are from 200 to 500 feet deep. The " coulees," as they are termed, form a curious feature of the third prairie steppe. These are valleys, or ravines, with steep sides, often one hundr^jd feet or more in depth, which terminate or close in, rather abruptly, often at both ends, forming a long trough-like depression; or one of the extremities of the coulee may open into the valley of a regular water-course. The coulees some- times run for miles, and are either quite dry or hold ponds of bitter water, which evaporate in the summer, and leave thin incrustations of snow-white alkaline salts. The average depth of the river-valleys of the first and second prai- rie steppes is not affected by the general descent of the country through which they run. From the Little Boggy creek to i/he Arrow river, the Assineboine must fall 400 or 500 feet, yet the banks ot* the valley maintain the same general height and the same character throughout the whole distance. Similarly, the fall in the Calling river, from the 8and-Hills lake to its junction with the Assineboine, can not be far from 500 feet, and still its valley-banks have the same average height throughout. The fall in the Red river, from Moorehead to Fort Garry, is upward of 200 feet; but in the whole of the distance, the banks of the river have a nearly uniform height of 20 to 30 feet. The great valleys of the third steppe cut entirely through the drift and far down into the underlying Tertiary and Cretaceous rocks; those of the second steppe appear to correspond, in a general way, with the depth of the drift, while on the lowest steppe, the streams have merely cut through the modified deposits resting upon the drift, which latter is occasionally exposed at low water at the foot of the banks, or in the bed of the stream at swift places and rapids. The stratified claj', silt, sand, and gravel of the Red river and the lower Assineboine, vary in thickness from almost nothing to 80 or 90 feet, and a variable thick- ness of bowlder clay is interposed between these deposits and the older Menozoic and CUnnozoic Geology and Palceonfoloyy. 325 far t-ry, of rift lose I the rely Ittei* Ithe Isilt, in ick- Ider rocks*, which lie beneath tlieni all. At one place, in sinkin*iirfacc cl(>va- tion of the country here is 100 to 200 feet al)ov(! I^iike ."Miciiigan, and the clays SO to 100 feet and over in depth, as sliown by luinierons Mitc- sian well l)orings that yield a flow of water which is obtained fi-oni soanis of gravel at different liorixous in the cla}'. The clay of eastern Waushara county is i)art of a large clay area that extends up the Green IJay valley from Lake Michigan, and it is quite significant, that Prof. Irving's map of this lake deposit shows that it extends within about twenty miles of the northeastern part of the ilriftless area of Wisconsin. Afterward* he said the lacustrine clays underlie all of the lower levels bordering Lake Superior, above which they rise to altitudes of between uOO and (500 feet. This carries them well up the front slope of tlie Copper range, and high, also, on the flanks of the liayfleld high- land. On the Wisconsin Central, these clays reach to an altitude of 500 feet, and are finally left, on ascending the railroad line from Lake Superior, near where Bad river is first struck. The clay varies largely in amount of sandy admixture. There is commonly some sand included, though, at times, it seems almost wholly absent, and at others to make up the bulk of the formation. The clayey matter is always of a red color, and always contains a considerable proportion of lime carbonate. The stratification is not always evident, but on the shore bluflfs of the Apostle islands, it may be seen in the darker color of the moist sandy layers as compared with the lighter sun-dried clay. In many places, numerous small bowlders, chiefly of some dark greenstone-like rock, are to be seen embedded in the cla}-, and pebbles of the same, and other crystalline rocks are abundant. On the shores of some of the Apostle islands, and in places along the mainland coast, dark-colored bowlders of large size, presumably washed out from the clay, are very abundant. The entire thickness of these clays can not be less than from 400 to GOO feet, about 100 feet being the greatest thickness seen in any one section. Mr. E. T. Sweet found a section of the lacustrine sands and clays, with gravel and bowlders, on the north bank of the St. Louis river, about one quarter of a mile from Greeley station, 202 feet in thickness. In the vicinity of Fon du Lac, and southeast of Superior Cit}^, along the old St. Paul military road, he found lake terraces at 15, :55, 80 and 120 feet above the present level of the lake, and an indistinct one at the * Geo. of Wisconsin, vol. iii. :J28 Tertiary. I hoi<;lil of ;!0(» feet. Aloii.ij[ tlu! IJriile riviM', in tlic vicinity of the rrioutli nt tiiL' Nobaj^iuimin, whert; tiio rlvor is .'JOO feet jibovo Lak«' Siiporioi* river terraeosi jire fouiul IJO, 80, jinil li)() feet above tlio I'iver. Fioin the top of the liighest terrace, or level of the Hurroiiiidiiig country, to the corrcMiJonding top on the opposite side of the valley, the distance is about a mile, 'J'hc lake terraces and lak»! deposits of sand and clay at these hei«>hts in Wisconsin, show that I^ak»; Superior has stood at a height sulllcient to have overflowed the highest lands in any of the States south of it. The driftloss region in the western half of the State, is jdikc conclusive against any of the drift phenomena in the eastern part, having been the result of glacial action of anj' kind, and they both unite In testify- ing against a continental ice sheet, or glacial period. In Dakota county, Minnesota, there occurs an outlier of the St. Pe- ter's sandstone, known as ''Lone Rock," owing to its standing in a prairie, and forming a conspicuous object for many miles in all direc- tions. Its summit is about one hundred feet higher than the sur- rounding country, and from this point a number of outliers and pin- nacled rocks of the same sandstone may be seen. One of these is called "Chimney Rock," from its fancied resemblance to a chimney; and another, standing seventy feet high above the surn iding coun- try, is known as " Castle Rock," the upper twenty feet of h is now so slender that but few centuries will pass before it totters auu falls, under the sve.vring effects of subarial denudation. These sandstone outliers aro monuments attesting the erosion which has taken place since Silu- rian times, and yet, in the valle3's of this county, the drift prevails and bowlders abound. In Wabasha county, we have the "Twin Mounds," and in Olmstead county, the "Sugar Loaf jNIound" and the "Lone Mound," and numerous isolated bluffs, attesting the erosion for the same period. In Fillmore count}', tlie Trenton Group forms precipit- ous bluffs. It rises perpendicularly from the short talus at the base, which adjoins the creek, forming canons, which widen as we descend the streams, and which, like the monuments of other counties, attest the erosion through long periods of time. The weathering and erosion have left manj' scenes in the bluffs of wild and picturesque beauty, as at Weisbeck's dam, in Spring valley, that, standing alone, or consid- ered in their relations to each other, as their bearing is found in all directions of the compass, are convincing proofs of the non-existence of the glacial epoch. But the strongest proof, it seems, that one could wish against the glacial speculation, may be seen in two lonely towers, Meno^oic 'Dul CcEHozofc Cienlofjii and PdhvontoUHjij, :120 in tlio valley of tlio soiitli brfincli of Root river, in this coiiiity, known tiH tlio " Ka^li! Roc'lvS." The vnllcy is one of (lemnlMlion, by tlu' onli- nnry subu'riai forces, and it lias been excavated out of tiie Trenton Group; and yet, two lone towers, risin<>; as liijjfli as the rocky walls of the valley, are standing to say that no glacial slioet ever tnoved in this vall(>y. IndecMl, no one havinj; any knowledge of geology, has fonnd any evi- dence of glacial action in the Mississipjii valley, (tr in the slreanis that flow into it from Minnesota; bnt, on the contrary, every geological fact bearing upon the snbject is so strongly against it, that we nidu'sita- tingly conclude that no glacier, great or small, ever entered it; and as to the hypothetical continental glacial sheet In this valley, it certainly suggests i)h3'sical impossibilities. Tito valley of the Mississippi is one of ei'osion. At Minisca, the hills are o^o feet high. 'V\\v. slo[)(>s arc such as are made by ordinary forces, without the intervention of anything extraordinary. The hardcsr layers of rock statid out in bold clifl's on the sides of the valley, while the softer layers form slopes b(>- tween the harder layers, marking the disintegration and denudation as it takes place under atmospheric inlluences. Streams enter the valley at right angles, and these are fed by streams flowing into them from the north and from the south in valleys of corresponding de[)th, and protected by sides of similar slopes and cliffs, and even more rugged bluffs; for, as we recede westerly from the Mississippi river in South- ern Minnesota, higher rocks come into view, until the valleys are exca- vated in the limestones of the Trenton Group, instead of the softer raf^gnesian limestones that abut upon the Mississippi valley. If a sheet of ice were to fill these valle3's above the top of the dividing ridges, we may fairly conclude that it would be held so firmly that it could move in no direction; but if it could move either north or south- or east or west, the sharp escarpments of magnesian limestone, the rugged bluffs of the Trenton limestone, the bold outliers in the widened valleys, and the pinnacled towers on the level prairies forming the divides between the streams, would be ground down, smoothed off, or entirely torn away. A trip up the Missiosippi river, from Dubuque, Iowa, to St. Paul, Minnesota, or across tlfe country at La Crosse, Minisca, or Lake Pepin, will bring to the view of the observer the incontestible evi- dences against the existence of a continenlsal glacier, in times so recent as the Pliocene or Post-pliocene. In the absence of the opportunit}' of taking the trip, turn to Owen's Geological Survey 330 Tertiary. ^^!li: I of Wisconsin, Iowa, and Minnesota, and look at the "Natural Section of Hills, Upper IMississippi;" " Cliff of Lower Magnesian Limestone, Plum Creek;" "Alterations of Magnesian Limestone and Sandstone, Kickapoo;" "Lagrange Mountain;" "Castellated appear- ance of Lower Magnesian Limestone, Upper Iowa;" "Lower Mag- nesian Limestone, Upper Iowa;" "Cliffs of Lower Magnesian Lime- stone, Upper Iowa River;" "Outlier of Sandstone, Kinnikiniek;" "Outcrop of Upper Magnesian Limestone and Shell Beds, Turkey River," and you will be enabled to form some idea of the bluffs, cliffs, castellated rocks, and pinnacled outliers, that are so utterly inconsistent with the glacial hj'pothesis. Such scenes are also presented in the State of Wisconsin, both within what is universall}' conceded to be the driftless area and without it- Two of these curious isolated eminences are situated in Dark Hollow, north of Wingville, on the head waters of the Blue river, near the junction of Badger Hollow, and composed of the Upper Sandstone, as illustrated in Hall's Geological Survej'. Another called the "Stard Rock," in the Dells of the Wisconsin, forms the frontispiece to Vol. ii. of Chamberlin's Surve3\ But Prof. R. D. Irving informs us that a remarkable feature of ail of the paloeozoic portion of central Wisconsin? is the occurrence of isolated ridges and 2^Qin it followed the streams westerly to the Alississippi, and from its eastern margin to the Oliio, so that its greatest width in these States exceeded ilOO miles. This overflow may have been prodnced by volcanic energies in the Lake Superior region, and occurred as late as the Post-pliocene age. It was the great destroyer of the mammoth and the mastodon and other extinct Post-pliocene mammalia. Since that period the lakes have gradually drained themselves to lower levels through the outlet at Lake Ontario, leaving here and there lower lake beaches and terraces. In process of time, Niagara Falls will recede to Lake Erie, and that lake will be drained to its ancient channel, and other beaches and terraces will be left to represent the present height of the lake in the same manner that I have supposed the higher beaches and terraces to represent the former levels. This explanation seems to the author suflicient to account for all the phenomena discovered by tlie geologists, and it certainly calls to its aid no mythical hypothesis or unknown freaks of nature, but rests upon well-known physical and geological laws. It is no small tax upon the imagination tr believe that a great sheet of ice, having an existence in the north, ascended the Laurentiau mountains north of these lakes, and then dipped down into the earth, scooping out Lake Superior 900 feet in depth, pulverizing the material, transforming it into gravel, sand and bowlders, scraping ofl the soil in some places, and scratching the rocks in others, as it ascended the valle\'s to the height of the dividing ridge between the waters that flowed to the north and the south, and precipitating itself into the tributaries of the Ohio, Mississippi and Missouri rivers, and depositing behind it in such even and beautiful distribution the sand and gravel that now fills the ancient valle\'s, and forms a vast, almost level plain over the northern pp.ts ot Ohio, Indiana and Illinois, and yet did not sweep off the ancient gravel beaches, in many places, that now mark upon the mountains and hills the ancient shores of vast bodies of water. To believe in the glacial theory requires all this stretch of the imagina- tion, and to be a real sound stalwart in the faith, there are many other marvelous things which must be accepted. One of these is described by a Pennsylvania geologist, to account for the drift phenomena of New York. He says : " But when the ice front had been melted back to the southerly crest i! 338 Tertiary. H u of the ClmutJiuqiKi divide, tiie battle between the elements of heat and cold commenced in earnest. North of the barrier, tlie ice-king had massed his forces; Lake Eric bnsin was full of ice, and all the reserves of the north were freely moving down into it. As fast as one skirmish line on the summit was repulsed, another was thrown forwai-d; and thus alternately advancing and retreating, the contest raged for ages before the invading ice was forced back, permanently confined, within the limits of the present lake basin." The Muse that divulged this information must have been slain in the last glacial engagement, and remained for ages housed up in her little sepulchre, because, otherwise, it is evident that she would have told all about the grand glacial ball which ensued after the vict()r3' was complete, when the glaciers danced quadrilles, waltzed and ma- zourkied, and scratched and furrowed the rocks in all directions, followed by cutting the "pigeonwing" and the great American " hoe-down," when the glaciers shook the gravel, sand and bowlders, which they had collected for war, out of their crests and huge de- l)ositories, and covered the earth, which in their great glee they had cut up and striated so beautifully. In conclusion, the author would seriousl}^ call the attention of the I'eader to the array of facts here collected tending to prove that there is no marine or other deposit which represents a glacial period of time, and, therefore, there is no such geological period; that there is no gap in geological nomenclature into which it can be lodged or injected. That the fossils and animal and vegetable remains teach us of no such period, but quite the contrary. And, finally, that the glacial epoch is a theoretical blunder, without the support of any known facts, and averse to all our geological and palreontological information. ^.b' r lieat nnd •king had le reserves I skirinisli vjinl; and 1 for tigCH ?a], witliin n slain in up in iier ould have le victorj' and nia- liroctions, American bowlders, huge de- they had 3n of the hat there period of here is no • injected, f no such spoch is a nd averse 'J' S'