SMITHSONIAN LIBRARIES SSIYVYRIT LIBRARIES fee SRO ROE Ne AS CS N,N oe em m SS NAS XGyy 5 ‘ai m aN Z m 2 ae ‘ S SMITHSONIAN INSTITUTION NOILNLILSNI _NVINOSHLINS (Sa luv ud 1 = z é = 4) < = / = z = bij = 4 AP ro) ae iy. 5 aa . D a ae yi 7) wo a = Wy ae: : > a . = a 2 a 2 i NI LIBRARIES SMITHSONIAN INSTITUTIOI 2 mh Z a = | a yn 7 as na 4 & = wz a = y - 4 | Gc te = = ce EN. co = fm. a O SS —s oO = [@) = 3 z a er { -S SMITHSONIAN INSTITUTION NOJLONLILSNI NVINOSHLINS S31yuVY at Gs 5 z ~ ; z o “00 9 ow xX Oo = Be i eB = Fe > = > e =e 2 = 20 = 2 m “ = w “= n z a Zz NI! wm wm = = = = A i AE wm ¢2) O Oo. = = 2 2 z Ve a NS < = “ tn” Z NY . 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ES SMITHSONIAN INSTITUTION NOILNLILSNI NVINOSHLINS SJ31luvus = i =z en SR Me KO eee me RS) ee Ta eas ees ges Published monthly by the BULLETIN 327 New York State Museum . University of the State of New York Bulletin 77 GEOLOGY 6 GEOLOGY OF THE VICINITY OF Pld TLE PALLS, HERKIMER COUNTY BY ti. P) CUSHING PAGE CU RUB KEE 2 dats Bact GoeeeOne on EomneeD ocdes 3 Geographic position..............-.....- 4 STI HD COLO Li aeccieinteis civics 0:c:0'<.slejeie sce cies 4 i TROCME Sgasb ac vGORe Ape One eo EE Dee enon 15 area OaMiOVIAMINOCIKS cs cesigiee cle oc. ee sieves 15 I EOZOIGIFOCIGS: oe clss less he vec tine sss cee 24 CUT) SCOLOLY cc... 2. ccc cette vs eee. 3D TDW Dino8 dab ek CU aa toese ACO oOsGRo apt ine sete 3B TAGIGEL BAAR AREA piohtee Aa GROEN pra i eae 37 FTIR EV ee aa Reco Cale actA Aen eae 38 SELOUTATTONM Sire. 'chc cp aahrcsievee ec alesis eosin a 47 JICHMUSAG NBN S.s haceiee sues oot Gaoe eRe eecEe 48 Some oscillations of lev al during the EV COZOICS oe 12 NEW YORK STATE MUSEUM which cut and are therefore younger than all the rocks of the region, up to and including the Utica formation. Their date can not be fixed more definitely than this. é On the south also there is evidence of igneous action of later date than the deposition of the Utica formation. A few dikes are found cutting this and the older rocks as well, which may or may not be of the same age as those of the Champlain valley. They are of a somewhat different sort of rock from any found there, and this may possibly argue for a difference in age. None of these dikes have been noted within the map limits, but three outcrop along Hast Canada creek just east of those limits. In character they show a closer relationship with some igneous rocks SS ——— = = _=s== = a <= Figure 4 * of apparent post-Devonian age which occur sparsely in central New York and they are probably related to them, rather than to the Champlain dikes. Since the deposition of the Potsdam, Beekmantown, Trenton and Utica formations, the region has also suffered deformation, which has affected them as well as the older rocks. This later deformation has not been severe however. The rocks are but Slightly folded, but are, on the other hand, considerably faulted and jointed This deformation period is of uncertain date except that it is later than the deposition of the rocks. Quite possibly *A fault is produced by a sliding movement of the rocks on opposite sides of a fissure, with the result that the same rock stratum is higher on one side than on the other, as illustrated in the accompanying diagram [fig.4]. The stratum AA has been dropped on the right side of the fault relative to its position on the left side. The distance ac, measured along the fault plane, is called its displacement, the vertical distance ab, that separates the two ends of the stratum, is called the throw, and the horizontal dis- tance be is the heave of the fault. GEOLOGY OF THE VICINITY OF LITTLE FALLS 18 the first faulting of the region took place at the close of the Lower Silurian coincidently with the Taconic disturbance. But, even so, a fault once formed constitutes a line of weakness, along which further faulting is likely to occur whenever the region ex- periences further disturbance. It is by no means unlikely that repeated slips have taken place along the fault planes since they were first formed. Two such faults, the Little Falls and the Dolgeville faults, are found within the limits of the map, and thence eastwardly faults. cross the Mohawk valley repeatedly. The Little Falls break is the most westerly one which has been detected in the State so far as the writer is aware, though it is not at all unlikely that small ones, at least, will be brought to light farther west. The Little Falls fault has a throw of nearly or quite 800 feet at Little Falls, and is hence of very respectable magnitude. There is another fault on lower East Canada creek, just beyond the map limits to the east. - The Little Falls district has been nearly or quite continuously above sea level for a long time; since Devonian time in all prob- ability and likely during a part of the Devonian also. The length of this period of time in years can be measured by no one with any degree of exactness, but a few million years are involved be- yond any question, and quite likely a good many million. During this time its surface has been undergoing wear instead of receiv- ing deposit. A considerable thickness of the rocks which mantled the surface as: it rose above the sea has since disappeared, and the present surface rocks are such because of the removal of what originally lay: above. Undoubtedly the shales of the Utica for- mation once covered the entire area. They have now disappeared from more than half of it. The Trenton has also been worn away from much of the surface, so has the Beekmantown, and the old floor of all these rocks has been eaten away somewhat in the locali- ties where it is now exposed at the surface. Such later formations as may have been deposited have been wholly removed. We can imagine them as replaced in their old position, since we know their order and thickness from their outcrops to the south, but 14 NEW YORK STATE MUSEUM we do not know at just what point to put the curb on our imagi- nation. The manner of progress of the wear on this land surface has depended on the rock characters and structures and must be left for later consideration. During this long time interval, the region has experienced changes of altitude, in part because of wear, in part because of up or down movements of the earth’s crust. We are as yet far from being able to trace out these movements. In times very recent comparatively, namely only some thou- sands of years ago, the district was covered by the ice sheet of the Glacial period. How long this condition persisted, how many times the ice came and went over the immediate region, we do not know. The advancing ice sheet removed the soil and loose rock from the surface and scoured away at the rock ledges be- neath. The retreating ice sheet spread a heavy mantle of deposit over the surface. The melting ice gave rise to streams and lakes which rehandled some of the glacially deposited material. The larger preglacial topographic features were little changed and remain today substantially as they were before the onset of the ice. The minor irregularities of the surface were largely obliter- ated however, mainly by the deposits laid down during retreat. The stream valleys were filled nearly or quite to the brim, and the modern streams are largely in new courses therefore, specially the smaller ones. Unequal valley filling, and unequal deposit elsewhere left hollows in the surface in which lakes now nestle, lakes which had no existence before the advent of the ice. The Mohawk valley lowland is a preglacial feature, but the preglacial divide between the east and west flowing streams in this lowland seems to have been at Little Falls, and was certainly not at Rome, its present position. After the ice, on its last northerly retreat, had uncovered the Mohawk valley but still lay across that of the St Lawrence, the drainage of the Great lakes passed to the sea by way of the Mohawk, the eastern end of the lake in the Ontario basin being at Rome. The present Mohawk is an insignificant stream as compared with its great predecessor, which has of, course left its mark on the valley. GEOLOGY OF THE VICINITY OF LITTLE FALLS 15 The time since the departure of the ice has been so compara- tively short, that the surface is substantially as the retreating glacier left it. During the retreat of the ice a slow movement of uplift was in progress in the region, and continued thereafter ; in fact there are strong reasons for the belief that it even yet continues. Because of this change the Little Falls region stands today at an elevation exceeding by from 250 to 300 feet what it had when the last ice lay on it. The streams of the region have either reexcavated their old yalleys or are engaged in cutting new ones, but the time is not sufficiently long to have enabled them to make great progress in the latter task. Besides, the recent rising movement of the region has constantly lowered the level to which the streams can cut. Even the Mohawk is not down to base level at Little Falls and elsewhere. Away from the streams the glacial topography has been but little changed. THE ROCKS Pre-Cambrian rocks! These ancient rocks are found at the surface over a large area occupying the northeast portion of the map, extending thence northward without a break through the entire Adirondack region. In addition, they appear at three disconnected localities, at Little Falls, Middleville, and at a spot locally known as the “ Gulf,” 24 miles northeast of Little Falls. The Little Falls and Middleville outliers. The pre-Cambrian rocks exposed at these two localities are identical, are quite homogeneous throughout, and are somewhat different in character from those exposed elsewhere. They are quite certainly old igneous rocks and belong to the syenite family of these rocks. They consist mainly of feldspar, always show some quartz, usually from 5¢ to 15% of the rock in quantity, and usually have only a small content of dark colored minerals, magnetite, horn- blende, pyroxene and black mica. These minerals form a granu- 1A more detailed and technical description of these rocks will be given in the closing pages of this report. 16 NEW YORK STATH MUSEUM Jar mosaic in which are set feldspar crystals of varying size, whose glittering cleavage faces, on freshly broken surfaces, form the most noticeable characteristic of the rock. At Middleville these are very abundant and large, often reaching an inch and more in length, and the rock is much the coarsest syenite that has been found anywhere in the Adirondack region. In fact, it very strongly resembles in appearance much of the igneous rock called anorthosite, which has wide extent in the eastern Adiron- dacks. Both are composed mainly of feldspar, but the feldspar is of-widely different character in the two.. That of the anortho- site is apt to show striations, looking like fine ruled, parallel scratches, on the bright cleavage faces, but such striations do not appear on the syenite feldspar.. The two differ much in chemical composition also. The syenite at Little Falls is more widely and much better exposed than at Middleville, is by no means so coarse, varies more in character from place to place, and in part shows no large feldspars whatever. As shown along the Little Falls and Dolge- ville Railroad, it was described in a previous report to the ‘state geologist South of the Mohawk it is more homogeneous | and more usually porphyritic than on the north side.2 The westerly exposures, in and about the city, show considerable red, fine grained, granitic rock cutting the syenite. This syenite has undergone extensive metamorphism, so that it has been rendered thoroughly gneissoid, and the finer grained portion of the original rock has been mostly, or wholly, re crystallized. The large feldspars also have been diminished in ‘size by the breaking away of fragments from their exteriors. In general the Little Falls rock is much finer grained and vastly more gneissoid than that at Middleville. In places at Little Falls the large feldspars themselves have been completely crushed to a mass of fragments, and drawn out into lens-shaped patches, around which the foliation curves, as it does also around the uncrushed, large feldspars. IN. Y. State Mus. 20th An. Rep’t, p.r83. °A porphyritic igneous rock is one which shows more or less numerous erystals, surrounded by more fimely crystalline, or even stony or glassy rock material. JSOM SUIYOO] ‘S[[BA [IIIT 1B o}1UOAS UBlIqumeBy-o1d JO Wyo oy} JO Mord ‘oJoyd “tassord “9 “p 1) unerng wnesny 93215 T 9381d GEOLOGY OF THE VICINITY OF LITTLE FALLS |. aly ~ Since these are small outliers and consist practically wholly of syenite, they can furnish no decisive evidence of the age of the syenite as compared with that of the other pre-Cambrian rocks. Tt has been stated that the Grenville rocks are closely involved with apparent igneous rocks which seem to have been either con- temporaneous with them or to have been intruded into them not long after their deposition. Also that at a later date there was a time of great igneous activity in the region, when huge masses. of molten rock were intruded into the Grenville rocks; and that at a third and much later time there was a further renewal of igneous activity, though in a minor degree. The writer’s dis- position is to regard the syenite under discussion as dating from the second of these periods, and as of much the same age as the the great syenite, anorthosite and gabbro masses of the central and eastern Adirondack region, but it should be emphasized that there is no decisive evidence in proof of this view. These two small areas are likely connected underneath and represent por- tions of the surface of the same mass, and it certainly represents a different intrusion from those in the heart of the woods, though regarded as belonging to the same group of intrusions. Diabase dike. The only representative of the third igneous period which has been discovered within the map limits, is a huge dike of the rock known as diabase, which is exposed about a half mile east of the Little Falls depot along the Dolgeville Railroad. The rock is black and fine grained, with many half inch, por- phyritic feldspars, of a general greenish gray, dull appearance because of alteration. Near the edges of the dike the rock be comes very black and dense and of stony texture, because of more rapid cooling and solidification there, due to the chilling effect of the walls. The dike is at least 120 feet in width, an unusually large size for these Adirondack dikes. Grenville rocks. In the main pre-Cambrian exposures within the map limits, rocks which are of apparent sedimentary origin, and hence classed as of Grenville age, play an important part. The extreme metamorphism which they have suffered has pro- duced complete recrystallization, with consequent disappearance 18 NEW YORK STATE MUSEUM of all traces of the original structures which characterize the sedimentary rocks. The argument for their sedimentary origin rests on their composition, mineralogic and chemical, and on their frequent variations in composition, beds of different original character having produced differing metamorphic rocks, whose comparatively sharp junctions look like old bedding planes. The most characteristic rocks of the Grenville series are the crystalline limestones, but these have not been found within the map limits. A single large boulder of impure crystalline lime- stone was noted on the surface of the heavy moraine which covers the district occupying the extreme north-central part of the map. As it is a soft and quite easily destroyed rock, these limestone boulders commonly indicate a parent ledge near at hand, here probably to the north, not far beyond the map limits. In the absence of limestone, the rocks regarded as characteris- tically Grenville comprise a series of light colored, often white gneisses,. very rich in quartz, interbanded with less quartzose rocks of darker color, and often with a very respectable percentage of black minerals, hornblende, black mica and magnetite. Both rocks contain, often in abundance, garnets of somewhat unusual color, a much lighter red than ordinary and with a vather pink tinge. These are more conspicuous in the dark rocks in general, but the light colored ones are seldom without them. They are commonly of about pinhead size but often run larger, specially in the darker rocks, those with diameters of from 14 to 144 inch being often quite numerous, and even larger ones are to be found. Another mineral which is very characteristic of these rocks and strongly indicative of their sedimentary origin, is graphite (black lead). Shining, metallic looking scales of this mineral occur frequently in the darker rocks, usually of sufficient size to be made out by the unaided eye. Another characteristic mineral, this time confined mainly to the light colored rocks and only visible under the microscope, is sillimanite. As has been said, the light colored rocks consist almost wholly of quartz and feldspar and are rich in quartz. Their composition GEOLOGY OF THH VICINITY OF LITTLE FALLS 19 would indicate that originally they were sandstones, generally more or less shaly. In many of them the quartz is now found in thin, regular leaves separated by very finely granular feldspar, and such “leaf gneisses,’ as Dr F. D. Adams of the Canadian Survey has happily styled them, are a very conspicuous feature of the Grenville rocks. However, the severe metamorphism to which most of the pre-Cambrian rocks have been subjected has recrystallized much of their quartz in the leaf form, both in those of igneous as well as in those of sedimentary origin, so that this character can not be regarded as in any sense indicative of origin. It is naturally best exhibited by rocks rich in quartz, and some rocks which were likely granites originally show it in great per- fection. The darker colored rocks would seem to have been shales and calcareous shales originally. They must have contained a small amount of carbonaceous matter, very possibly of organic origin, now metamorphosed to graphite. Many ordinary shales and lime- ' stones contain carbonaceous matter, so that the supposition is a very natural one. These Grenville rocks are very like rocks which Kemp has recently described from Warren and Washington counties, to the eastward, where they also occur in abundance, and where limestone is relatively scarce. From the standpoint of one who is familiar with but one of the two districts and necessarily depending on descriptions for a knowledge of the other, the rocks would seem identical in the two areas, and not unlikely the whole pre-Cambrian fringe on the south side of the Adirondacks will be found to be characterized by abundant Grenville rocks with a scarcity of limestone. Probable igneous rocks associated with the Grenville. At most of the Grenville exposures of any extent, rocks which are regarded as igneous are found mingled with them. They are always thoroughly gneissoid and are interbanded with the old sediments. They are thought to represent old dikes and sheets of igneous rock, possibly surface flows also, which were formed during, or not long after the deposition of the sediments, and 20 NEW YORK STATE MUSEUM which have been recrystallized and stretched out into rude parallelism with the sedimentary beds as a result of severe metamorphism. Though of somewhat variable nature, they present three main types: 1 Red gneisses which have the mineralogy of granites, and are thought to have corresponding chemical composition also, though they have not been analyzed. They are usually fine grained and with quartz of a pronounced leaf type. 2 Black, hornblende gneisses, sometimes with pyroxene also and usually with black mica (biotite), which have the composi- tion of gabbros or diabases. 3 Greenish gray gneisses, which have somewhat the color and appearance of very gneissoid varieties of the syenite previously described, and are very difficult to distinguish from them when occurring alone. They are commonly very quartzose, more so than the usual syenite, and very distinctly of the “leaf gneiss ” type. They are very like the red gneisses of the first type under ‘ the microscope, have the mineralogy of granites, or of quartz Syenites, and are regarded as igneous rocks. Their possible re- lationship with the Little Falls syenite is an exceedingly difficult problem, not as yet satisfactorily solved, though they are hesi- tatingly regarded as distinct and as older. Though all these rocks are usually found interbanded with the Grenville sediments, so that there can be little doubt as to their close association, they may occur elsewhere unaccompanied by the sedimentaries, or with these in very minor quantity, and such areas have been given a separate coloration on the map, though the distinction is not a sharp one, and there is some question as to its wisdom. Syenite gneiss. There is a considerable area shown in the north- eastern part of the map where the rock is of the same sort through- out. The exposures are all in the woods and of the unsatisfactory sort that obtain there. The rock is thoroughly gneissoid, of a greenish color and weathers rapidly to a dingy brown. Most of the exposures show nothing but the brown rock, though usually GEOLOGY OF THE VICINITY OF LITTLE FALLS 21 freshly broken surfaces will show at least patches of the green. The grain is usually quite fine, but the quartz is coarser than the other constituents and tends often to the “leaf” type, though but rudely so. In places a few larger feldspars show also and appear like small examples of porphyritic feldspars. The rock is prevailingly of feldspar, and feldspar of an acid type. It is quite quartzose, that mineral making from 15¢ to 204 of the rock on the average with a usual range of from 102 to 30%. Pyroxenes are the usual dark colored constituents, though both hornblende and biotite mica also occur. Without going into detail at this point suffice it to say that the rock has the precise mineralogy of an augite syenite, the same mineralogy as the rock at Little Falls and Middleville, and the same as the great mid-Adirondack Syenite masses. It differs from them in being in general some- what more quartzose, in being everywhere thoroughly gneissoid, and in the lack of porphyritic feldspars. It is however not to be in any way distinguished from some varieties of the rock in the other exposures. On the other hand, it has nearly, if not quite, as strong a resemblance to the greenish gneisses, (3) just previously described. Mixed rocks about the syenite. A large part of the pre-Cambrian area of the sheet shows rocks which are very like the syenite rocks and are thought to represent phases of them, but which are in- extricably intermingled with smaller masses of undoubted Gren- ville rocks. The syenitic rocks predominate, though they are not of the normal type, but the Grenville rocks are in considerable force, and the relations between the two are wholly obscure. It was found impossible to separate the two in mapping on this scale, and therefore the complex as a whole is given a separate coloration. on the map. Since the rocks seem to pass into the syenites on the one hand, and into belts in which the Grenville sediments preponderate on the other, the mapping of boundaries must, however, be a wholly arbitrary matter. : A very mixed lot of rocks is found in this belt as mapped, and with frequent changes from one sort to another. The most abundant type of all is a greenish gneiss, weathering brown. 2 NEW YORK STATE MUSEUM which is richer in biotite, hornblende and pyroxene than the usual syenite. Metamorphism has concentrated these minerals. along certain planes, producing a marked gneissoid structure, and a rock varying from green to black in general color. Where thus: enriched by these minerals the rock approaches more nearly to & gabbro in composition, otherwise it is a syenite, though often very quartzose. With the increase in the quartz percentage the color often changes with facility from green to red and back again, just such a color change as is often seen in the great Adirondack masses of syenite. Bands of very basic feldspar, hornblende, biotite gneisses occur frequently with the others, and the whole series is cut by a multitude of small veins of quartz and pegmatite. Rocks like these appear in a multitude of exposures. All have the mineralogy of igneous rocks and are believed to be such. Along with these a rock repeatedly occurs which resembles some- what the green and black gneiss of the above, but contains earnets numerously also. It has the mineralogy of a rather basic igneous. vock, neither a gabbro nor a syenite however, but of a rock interme- diate between them and known as monzonite. It passes on the one hand into the syenite gneisses and on the other into the darker. colored gneisses, often with graphite, of the Grenville series, the lighter colored gneisses appearing with these at times also. The whole series is perplexing and uncertain. The rocks differ con- siderably from the red, black and green gneisses previously de- scribed and regarded as igneous rocks of Grenville age. SY Se) | Ma I IIL MEM he WING LION So AOL Im A er ELA —— oe Sa om Sp en £46 ar me ei . fand v8 I With DIVISI' il. p =! Catalo of 18 Handb In qu HS Ni Outlir H13 f Brief biology; H15 | 124f Ttine1 for the classic t H16 Ff H17 F H18 [| H19 ¢ Maps. Yor v. I Tssuec « % : STATE MUSBUM BULLETIN 77 UNIVERSITY OF THE STATE OF NEW YORK UTTLE FALLS QUADRANGLE Fe : : : > Terai LEGEND ‘SEDIMENTARY ROCKS Modernvalley allu- vium and marstide posits with some cial sandand grave benches andunder: lying Ulin ie Mohawk and West Canada valleys PLEISTOCENE best 950°C 3% Pleistocene unclassified concealing Boundaries Lorraine formation; Utica black shales, with thin loyers of slaty lime stoneinloworportion =a Trenton-Utica passage beds) alternating layers of black shalejand thin black, blocky limestone LOWER SILURIAN and Black River lime- stonos atthe base; moally gra yand black jo thinbeddedlimestone Beelamantown formation, Little Falls dolomite; massive, grey, often. sandy dolomi various gneisses and schists mostly quartzosc) usually containing Samet and frequently graphite IGNEOUS ROCKS PRE-CAMBRIAN [a] Diabase,onlyin dikes; Tate pre-Cambrian PRE-CAMBRIAN sid) ofpost- ‘age but mucholderthan the diabase (Laacetisy ROCKS OFUNCERTAIN QRIGIN Mostly red granite andblackamphibolitic gneisses probably igneous Sormewhatinvolyadyyith Grenville sedinentsand| probably of Grenville age TAN y Sneissoid sye iss, somewhat éled with granitic IB gneisses, and with patches of basic gar- neuferous gneisses that may be tory inclusions. The * others appear to bois - neous probably amixed border zono ofthe syenite UNKNOWN PRE- CAMBRIAN Pre Cambrian but of unknown character because concoaled heavy drift PRE-CAMBR Faults t Tron ore mine e Stone quarries AB. CD. EF and GH. are lines of Secuons. ‘00 er H.M Wilson, Geographer in charge. teh weed by Nastate Survey and Hersey Munroe. i | fo} Lovell, CC Bassett and Hersey Munroe. i Buveyed inf898\in cooperstion with he State of NewYork, 4 H ey S o 1 2 a a 5 Glometers H rr 4 Contemr interval 20 feet. 7 Approxiunre Mean DECLINATION 180% ~ Dertsun ts man sect tavel- Ss = as il Faul Lj (G1 IN ID) Z Se SaVMeEN nARY ROCKS IGNEOUS ROCKS LOWER SILURIAN PRE-CAMBRIAN PRE-CAMBRIAN a il Faults University of the State of New York New York State Museum _ The New York State Museum as at present organized is the outgrowth of the Natural History Survey of the State commenced in 1836. This was established at the expressed wish of the people to have some definite and positive knowledge of the mineral resources and of the vegetable and animal forms of the State. This wish was stated in memorials presented to the Legislature in 1834 by the Albany Institute and in 1835 by the American Institute of New York city and as a result of these and other influences the Legislature of 1835 passed a resolution requesting the sec- retary of state to report to that body a plan for ‘“‘a complete geological survey of the State, which shall furnish a scientific and perfect account of its rocks, soils and materials and of their localities; a list of its minera- logical, botanical and zoological productions and provide for procuring and preserving specimens of the same; etc.” Pursuant to this request, Hon. John A. Dix, then secretary of state, presented to the Legislature of 1836 a report proposing a plan for a com- plete geologic, botanic and zoologic survey of the State. This report was adopted by the Legislature then in session and the governor was “authorized to employ competent persons to carry out the plan which was at once put into effect. The scientific staff of the Natural History Survey of 1836 consisted of John Torrey, botanist; James E. DeKay, zoologist; Lewis C. Beck, mineralogist; W. W. Mather, Ebenezer Emmons, Lardner Vanuxem and Timothy A. Conrad, geologists. In 1837 Professor Conrad was made paleontologist and James Hall, who had been an assistant to Professor Emmons, was appointed geologist to succeed Professor Vanuxem, who took Professor Conrad’s place. The heads of the several departments reported annually to the gover- nor the results of their investigations, and these constituted the annual octavo reports which were published from 1837 to 1841. The final reports were published in quarto form, beginning at the close of the field work in 1841, and 3000 sets have been distributed, comprising four vol- umes of geology, one of mineralogy, two of botany, five of zoology, five of agriculture, and eight of paleontology. : ©. = oc a o < % = < ae < oe S oe c a = rs) as 3S a ar 2 nf > Sey S3!1yYVvVYuYgIT LIBRARIES SMITHSONIAN | oi = Hi : eS iS i w = a 2 wo 2 : E 2 > = > es ~ cad i cd Sin We om RA = m Ne i m9 wo = w z no 4 B RARI ES SMITHSONIAN INSTITUTION NOILALILSNI _ NVINOSHLINS Sa 1 : = Z = gy, : = 5 z 5 @% 2 I 3g 8 WOE? S e = S) Gf oe e 2 = >" = > = ” Zz 7) 2 _NVINOSHLINS LIBRARIES SMITHSONIAN INST a us z ul Dp ae za ao “i . Yin? = _< ra < Df at cS foe eG wo is WE 4g, [ omg = co 7 a gps oS re) a ro) otrasas Oo : = er DES iy eae IBRARIES SMITHSONIAN. 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