SMITHSONIAN LIBRARIES (a - am 7 > cm (cual YY fo fa amt Tuy) S WY e ew Ss Ry) = OY § Os So a: co Os > pa is KS mo.” F ; = Wasi’ Oo oe WAsts oO INOSHS sas re) = ond |. = oJ = 3RARIES SMITHSONIAN INSTITUTION NOILNLILSNI NVINOSHLINS S3I1uvugt" ae ™ a. ay es ; S a) o mt ) uc - ny ~ a re “a - is “i > a - Pao . S el a Z o z , a f ILALILSNI SAIYVUdII_ LIBRARIES SMITHSONIAN INSTITUTIO = 2) = wee w = 2 ‘' (i = <4 ba; 5 SAY Ye po. = ‘ae 2 iG ‘My 3 X. <4 is Oo | . ) ie a & Yy = UG o Co FE Z Gy Ee a = — ca - ~ > — a a Lye = SMITHSONIAN __INSTITUTION NOILALILSNI NVINOSHLIWS ” z ” = ae ” ta iat AS lu : 4g ; Z WX = <* + x 4 RX \ = as > di = > : ; a 7) ‘Pe Po ” = a _ NVINOSHLIWS S31iuvVYg ten BRARIES SMITHSONIAN INSTITUT - ie = ed > “2 4 ae 4 =e ao . oe | fave c o Cc Ee rae] oe 4 Oo ” aN tas! 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Ka uJ USVAT >) = af ft (ete = TH 2 WS — (Set wy) SONNE Ga 5 Gu) FZ 5 ey | Sy Oo >S oo “ wasn: Oo biNosy m 7 Oo Lr MESS c ; Zz iit a) Zz er 2 ; AR I ere cen eT TU TION NOILNLILSNI NVINOSHLINS S31yNvug ap 7 z ‘- ms = = ; . = = salle 5 : = = a E bh = F = = 1 2SNI_NVINOSHLINS S3 1uYvud roti BRARI ES SMITHSONIAN INSTITUTION, FES = = @& = t geouu z ae i fy z WZ \ = = : (2) i Jb ty O Ms. & pa ro) 2 2 Gd tN 3 2 : E 2G = n 2 : : ; : Baty ; 2 ARIES SMITHSONIAN INSTITUTION NOILNLILSNI NVINOSHLIWS S314v4SIT RARIES S INSTITUTION NOILNLILSNI LIBRARIES S3IYVYEIT LIBRARIES INSTITUTION I'1 LIBRARIES VUgIT_LIB ‘@ § gS z (e) Ww 4 Yt sTITy * or 4 Gy INSTITUTION NOILNLILSNI Sa1uvygly saiuvug TAILC TITLITICVAL INSTITUTION NOILNLILSNI NVINOSHLINS S3IYVUSIT : NVINOSHLINS S314 SMITHSONIAN NVINOSHLIWS NVINOSHLIWS WY SMITHSONIAN x WN SS , : LILSNI NVINOSHLIWS LIBRARIES SMITHSONIAN INSTITUTION IIRDADIC CC CAAITLICMAIIAAI NOILNLILSNI NOILNLILSNI LIBRARIES SS CAS HLA INSTITUTION NOILNLILSNI INSTITUTION NOILNLILSNI NVINOSHLIWS ARIES SMITHSONIAN S3AluVvugit INSTITUTION INSTITUTION AILSNI NVINOSHLINS S S3IYVYUGIT LIBRARIES S3I1YVUSIT LIBRARIES SMITHSONIAN ». ARIES SMITHSONIAN INSTITUTION NOILALILSNI NVINOSHLIWS : > a ; rT) CEMSONTS SAMS > ANS PEP ee te fe VIN LTP 2 WS 1 NVINOSHLINS S3SIYVYEIT NVWINOCUIIAC cuaurwuwwarr SMITHSONIAN NVINOSHLIW SMITHSONIAN sa1uvugin .1ES SMITHSONIAN RIES RIES ICNT LSNI DP ¥ h tly. by the University of the ‘State of New York -class matter June 24, 1908, on tis Post Office at ska gta N. Y., under = ; the act of July 16, 1894 ALBANY, a eaten FEBRUARY I, 1909 = New York State Museum — Joun M. Crarxe, Director Museum bulletin 126 pes TRENTON FALLS AND VICINITY IN _ ONBIDA AND HERKIMER COUNTIES BY : W.J. MILLER % PAGE The Precambric surface... ..... 35 é Absence of the Dolgeville = hy and drainage. . Sear | Trenton) shales 37 f the region. irc. 2 Set Eg Glacial geology ....,..... 30 ) al features. ee E Economic geology ey 46 | 49 e ALBANY NI VE SRSITY OF THE STATE OF NEW YO a DO ems aa Tr \ “20 04583 a) sRoael Wuse joe . a —— STATE OF NEW YORK _ EDUCATION DEPARTMENT Regents of the University With years when terms expire - 1913 WHITELAW Rep M. A: LL. D,-D.C.L. Chancellor - New York — 1917 ST Ciain McKetway M.A. LL.D. Vice Chancel- 4 Jor) - Se aa -.- 2 23 oo 1919 DaniEL BEACH Ph. D. EE D. -»- - - - - - Watkins “1914 Puiny T. Szexton LL.B. LL.D. - - - - = = Patiigera 1912 T. GuitForD Smith M.A. C.E. LU.D. - - - Buffalo 1918 WILLIAM NotTTincHAM M.A. Ph.D. LL.D. - -Syracuse — 1g10 CHARLES A. GARDINER Ph.D. = H. DD. Eee 4 DC ee ee - - - - New York | 1915 ALBERT VANDER VEER M.D. M. ne Ph. De Sige D. Albany 1911 EpwarD LAUTERBACH M.A. LL.D. - - - - - New York | 1909 EUGENE A. Puitpin LL.B. LL.D. - - - - - New York — r916-Lucian L. SHEDDEN LL.B: LUD. ee '- Plattsburg — Commissioner of Education ANDREW S. DRAPER Lis. -bEae Assistant Commissioners Aveustus S$. Downine M.A. Pd.D. LL.D. First Assistant Frank Ro.uins B.A. Ph.D. Second Assistant Tuomas E. Finecan M.A. 7hird Assistant Director of State Library James I. Wver, Jr, M.L.S. Director of Science and State Museum Joun M. Crarke Ph.D. LL.D. © Chiefs of Divisions © Administration, Hartan H. Horner B.A. Attendance, James D. SuLiivan Educational Extension, WiLL1am R. Eastman M.A. MLL. ae Examinations, Chee F. Wueevock B.S. LL.D. Inspections, Frank H. Woop M.A. : Law, FRANK B. GILBERT B.A. School Libraries, CHaRLES E. Fitcu L.H.D. Statistics, Hiram C.. Case Trades Schools, ARTHUR D. DEAN B.S. Visual Instruction, DELANcrEY M. EL.is New York State Education Department Science Division, July 2, 1908 Hon. Andrew S. Draper LL.D. Commissioner of Education Sir: I have the honor to communicate herewith for publication ‘as a bulletin of the State Museum, a report on the Geology of the Remsen Quadrangle, including the Vicinity of Trenton Falls, N. Y., accompanied by a geologic map of the region. The work has been prepared by Prof. W. J. Miller of the staff of this division. Very respectfully Joun M. CLARKE Dvtrector State of New York Education Department COMMISSIONER'S ROOM Approved for publication this 3d day of July 1908 Jaiow: Commissioner of Education % : 3 : 4 . M s = 2, Ss “ . , S i ‘ Rs . ‘ , A i + ; ‘ 7 F 4 Z é , . « i : - » . “ : ’ SA 4 i r / ™* . ~ . ‘ i a r . < - - + ’ é . - 2 - ’ 3 <—s * i al Education Department Bulletin Published fortnightly by the University of the State of New York Entered as second class matter June 24, 1908, at the Post Office at Aibany, N. Y., under the act of Congress July 16, 1894 No. 440 ALBANY, N. Y. FEBRUARY I, I19¢9 New York State Museum Joun M. CrarKke, Director Museum bulletin 126 GEOLOGY OF THE REMSEN QUADRANGLE ‘INCLUDING TRENTON FALLS AND VICINITY IN ONEIDA AND HERKIMER COUNTIES BY W. J. MILLER INTRODUCTION The territory described in this report is covered by the Remsen - quadrangle of the United States Geological Survey. The map covers 7; square degree and lies between latitude lines 43° 15’ and 43° 30’ north, and between longitude lines 75° and 75° 15’ west. The region, partly in Oneida and partly in Herkimer county, lies along the southwestern border of the Adirondacks. The map represents nearly 216 square miles of territory and includes the type locality of the classic Trenton limestone formation. The gorge at Trenton Falls has long been famous both for its scenic beauty and because of the interesting geological section there shown. The whole territory was formerly heavily forested, but at the present time the woods are confined almost entirely to the north- eastern part and even there much of the timber is of second growth. A number of sawmills are now in operation as at Nichol’s Mill, Cs 6 NEW YORK STATE MUSEUM Forestport, Remsen, Bardwell Mill, one on Little Black creek, Northwood, Grant, and a large pulp mill at Hinckley, within the territory. The southwestern half of the region is devoted pri- marily to agriculture and dairying. GENERAL GEOLOGIC FEATURES Under this heading it is proposed to briefly outline the geologic history of the whole Adirondack region so that the detailed study presented in this report may be made more intelligible to the reader. — This outline is largely based on the admirable treatises of Prof. H. P. Cushing. So far as known the oldest rocks of the Adirondacks are those of Grenville (Precambric) age. They are sedimentary rocks, origin- ally shales, sandstones and limestones, which have been highly metamorphosed into gneisses and crystalline limestone. These rocks are of unknown though great thickness, and are widely scattered throughout the Adirondacks; thus showing that the whole region was under water at the time of their deposition. After the deposition of the Grenville sediments the region was raised above the ocean level and the rocks began to decompose and suffer erosion. Either just before, during or after the uplift, » great masses of igneous rocks were intruded. The Grenville rocks were for the most part engulfed by the intrusion so that only occasional patches of them were left intact. After the igneous activity the rocks became thoroughly meta-— morphosed by being squeezed, highly folded and converted into gneisses. Such changes can take place only at great depths (several thousand feet) and hence we are led to the belief that a vast erosion of the original land masses must have taken place. This in turn signifies that the land masses must have remained above sea level for an immense length of time. | | At or toward the close of this long period of erosion, igneous activity of a minor character took place. The basic igneous rocks erapted at this time are especially well shown in the north- eastern Adirondacks where they were squeezed up between joint. planes in the older rocks. That these rocks are much younger than the igneous rocks first mentioned is clearly shown by. their mode of occurrence .d their general lack of metamorphism. At the conclusion of the erosion period the region of the Adiron- dacks was nearer the sea level and of slighter relief than at present. Then the whole region began to sink slowly, allowing the sea to encroach upon the land until only an island was left or probably hie Aaah. Aelia GEOLOGY OF THE REMSEN QUADRANGLE 7 even until the whole region was under water. During the subsid- dence, deposition of Paleozoic sediments went on, one layer above another, the younger deposits overlapping each other and encroach- ing upon the sinking land surface. Since the subsidence was not entirely uniform on all sides certain local variations in deposition occurred. The first of the deposits to form upon the sinking floor was the Potsdam (Cambric) sandstone now found exposed nearly every- where except along the southwest border. After this the sediments changed in character and the limestones of the Beekmantown (Lower Siluric) were laid down. Then followed the deposition of the highly fossiliferous Trenton (Lower Siluric) limestones, including the Lowville and the Black River limestones. The fairly clear waters fullof animallife then gave way to the muddy waters of the Utica, when the Utica shales (Lower Siluric) were deposited. At this time the Adirondack region was probably all under water. Next came an uplift on the east and northeast where deposition ceased. Onthe south and southwest, however, deposi- tion continued and the successive formations of the Siluric and Devonic above the Utica shale were laid down. These Paleozoic formations may now be seen as one passes from the Adirondacks southward to the southern border of the State. The last period of igneous activity in the Adirondacks occurred some time after the close of the Lower Siluric. This activity was of minor extent and showed itself in the form of dikes. At some time after the deposition of the Utica shale the rocks, especially along the southern border, were deformed chiefly by faulting. A series of these faults extends across the Mohawk valley, a small one being present within the limits of the Remsen quad- rangle. The southern Adirondacks, including the Trenton Falls district, have been subjected to erosion for a vast length of time, certainly since the close of the Paleozoic and more than likely since the Devonic. During this great lapse of time a large amount of material has been removed. Doubtless the whole Remsen quad- rangle was at one time covered by the Utica shales, which have all been removed except along the western side. The superficial deposits, such as sands, gravels and clays, which are sO common over the Trenton Falls district were deposited either directly or indirectly by the great ice sheet of the Glacial age. From the geological standpoint this ice sheet was present only quite recently and covered most of New York State. 8 NEW YORK STATE MUSEUM TOPOGRAPHY AND DRAINAGE f¥ The region of the Remsen quadrangle presents a very ancient topography since it has been above water and subjected to erosion at least since the close of the Paleozoic era. The major topo- graphic ‘features are the result of this long continued wear, but the whole region has been thoroughly glaciated, and the detailed sur- face configuration has often been quite appreciably affected by the accumulation of glacial drift. The region is a characteristically hilly one, with the greatest difference in altitude above sea level being from a little over 700 feet, where West Canada creek leaves the map, to nearly 1900 feet in the extreme northeastern portion, where several points reach to and above the 1800 foot level. Extending northeastward from a line passing through Forestport and Grant, to the highlands just mentioned, there is a gradual upward slope which continues into the Adirondacks. In fact these highlands may be looked upon as foothills of the Adirondacks. Minor highlands occur in the west-central part of the district where the culminating point is Starr hill over 1780 feet above sea level. From Starr hill southward the general slope is towards the Mohawk ~ ‘river. As Professor Brigham has said, the magnificient view from the top of this hill strongly impresses one with the greatness of the Mohawk valley as a topographic feature. The country lying between the two highland areas is mostly drift covered and shows usual elevations of from 1100 to 1400 feet. The central and southeastern parts of the quadrangle are deeply drift covered, the drift ranging from 100 to 300 or 4oo feet deep and the hill tops ranging from 1300 to 1500 feet above the sea level. The principal streams are Black river and West Canada creek, . the latter stream being the chief tributary of the upper Mohawk river. These two streams present some of the most interesting drainage features of the southwestern Adirondacks. They have their sources close together in the Adirondacks and they flow southwestward approximately parallel for 30 or 40 miles to within the map limits where a striking divergence occurs. Black river turns northwestward or at right angles to its upper course, while West Canada creek turns southeastward and also at right angles to its upper course. At one point within the map limits the two streams are but little more than 4 milesapart. Black river continues northwestward to Carthage and thence westward into Lake Ontario; while West Canada creek continues southeastward and southward 3 } | : “5 q] J d > { } i GEOLOGY OF THE REMSEN QUADRANGLE 9 to empty into the Mohawk river at Herkimer. Thus Black river forms a part of the St Lawrence drainage system while West Canada creek forms a part of the Mohawk-Hudson system. Another striking but well known feature of Black river is the fact that it follows close to the Paleozoic-Precambric contact for 5 many miles. Doubtless the character of the Paleozoic rocks (mostly limestones) has had much to do with the determination of its course _ __ along this line. The main tributaries of Black river within the map limits are Big and Little Woodhull creeks on the north and Little Black creek on the south. The main branch of West Canada creek on the north is Town Line (Cincinnati) creek and on the south Black creek. Certain other topographic and drainage features are discussed in the following pages. ROCKS OF THE REGION The rocks of the region include Precambric crystallines and - Paleozoic sedimentaries. Each of these rock classes occupies approximately one half the area and they are separated on the geologic map by a line running southeast and northwest. The Precambric rocks represent a portion of the great Adirondack crystalline mass along its southwestern border. The Paleozoic rocks are of Lower Siluric age and overlap on the crystallines. Precambric rocks Grenville gneiss. Rocks of Grenville age comprise a series of highly metamorphosed sediments and they occur in but one well defined area within the map limits. This area, nearly triangular in shape, covers several square miles and extends from Enos south and southwestward. The best exposures are in the vicinity of Enos where for about a mile downstream Black river has cut a gorge through the Grenville rocks which are finely exposed. Another large outcrop may be seen where a road crosses Little Black creek about a mile and a half from its mouth. Grenville rocks have been found in many other parts of the region but they are so thoroughly involved with syenitic masses that they can not be separately shown on the geologic map. Where the Grenville rocks are found in considerable areas in the northwestern Adirondacks, crystalline limestones are commonly associated with them, and the limestone proves the original sedi- mentary character of the formation. These characteristic crystal- line limestones have not been found in the region here described. IO : NEW YORK STATE MUSEUM They have recently been found in the adjoining Little Falls dis- trict.1 Cushing notes the presence of limestone boulders near the northern edge of the Little Falls sheet which makes it probable that the limestone occurs on the Wilmurt sheet which lies east of the Remsen sheet. Another occurrence is at Fourth lake of the Fulton chain.? Thus it appears that the Grenville limestones are only poorly developed along the southwestern border of the Adiron- dacks. The strongest evidence for the original sedimentary character of the Grenville rocks within the Remsen quadrangle is the fact that layers of very different composition and color are in sharp ~ contact and often show rapid alternations. Such phenomena are — well exhibited in the Black river gorge at Enos, where the rock layers stand in almost vertical position and strike n. 7o° e. Near -the old mill there are many layers of very light color made up almost entirely of feldspar and quartz. These rocks must orig- inally have been beds of feldspathic sandstone and it appears probable that the present banding corresponds closely to the former stratification of the sandstone. These light colored layers are clearly interbedded with dark gray and almost black feld- spathic and hornblendic or biotitic rocks. Although some of these darker rocks appear to be of igneous origin and closely asso- ciated with the Grenville, nevertheless many of them are more than likely of sedimentary origin and were pS originally shales. Another strong evidence for the sedimentary origin of the Gren- ville rocks is the presence of graphite in them. Graphite flakes often a millimeter or more across and exhibiting a shiny metallic luster are very common in certain of the lighter gray layers near the mill at Enos. More rarely the graphite occurs in the darker layers. It 1s difficult to account for the graphite except on the basis of organic origin. Thus we may argue that the original sandstones and shales were more or less carbonaceous and during the process of inetamorphism the organic matter was ha and . crystallized into graphite. ' Another mineral suggesting a sedimentary origin which is often found in light red crystals, especially in the darker layers, is garnet. Garnets are rather more frequently present in metamorphic rocks - of sedimentary origin and their presence here, often in abundance, seems to suggest such an origin for the Grenville. 1 Professor Cushing has called the writer’s attention ine the discovery of this limestone y Newland. See N. Y. State Mus. Bul. 119. p. 14 2 Smyt th, C. H. jr. Crystalline Rocks of the Wiectee ‘Adicondaales: N. Y. State Mus. 51st An. Rep’t, Vize 897s ee ee = oe © eS EE GEOLOGY OF THE REMSEN QUADRANGLE II The Grenville presents many different facies and below follows a description of the principal types which are represented by different layers. A common type is distinctly marked by alter- nating light and dark bands, the light bands consisting mostly of plagioclase feldspar and quartz, while the dark bands are chiefly biotite mica and hornblende together with garnet. ! Another type is of light gray to greenish gray color and rather fine grained. The principal constituent is augite with a fair amount of anorthoclase and quartz together with several per cent of gra- phite. A third type shows a very thin banding, is almost white and is made up chiefly of plagioclase (oligoclase) feldspar with some quartz. A fourth type is fine to medium, light colored, and is made up of about 75% of anorthoclase, 20% of quartz and 5% of biotite, magnetite and garnet. , A fifth type is dark gray micaceous, consisting of about 60% of oligoclase, 25% of biotite mica, 10% of quartz and a little mag- netite and hornblende. A sixth type, which is rare, consists mostly of enstatite (or bronzite) with some quartz. A seventh type contains much sillimanite accompanied by anorthoclase, quartz, magnetite and biotite. The sillimanite occurs in long glistening needles visible to the naked eye. This type was observed only near Forestport, where Grenville and syenite rocks are closely associated. Accompanying the above described Grenville rocks and inter- banded with them are certain rock types which are presumably igneous in origin. One of these rock types is gray, medium grained . and consists of about 50% of feldspar — anorthoclase and oligo- clase — 25 to 30% of quartz, varying amounts of hornblende, hypersthene, biotite mica, magnetite, and a little pyrite, apatite and zircon. Found alone in the field it would be impossible to dis- tinguish this rock from the typical syenite below described. Another of these rocks thought to be igneous in origin is black, fine grained and highly banded. It consists chiefly of hornblende (so to 60%) associated with plagioclase feldspar (30 to 40%) which ranges from oligoclase to labradorite and about 5% of mag- netite. According to the composition the original rock would have been a gabbro. These apparently igneous rocks can in no case be represented as separate areas upon the map. Since the rocks of the Grenville series have been so profoundly I2 NEW YORK STATE MUSEUM changed by metamorphism, it is possible that the rocks above referred to as igneous may not be igneous at all, while others not referred to as igneous may in reality be igneous. Nevertheless most of the rocks of the series appear to be of undoubtable sedi- mentary origin. | Syenite gneiss. A considerable portion of the region mapped as Precambric is made up of a rock which shows every indication of being truly igneous in origin. Also its areal distribution and relation to the Grenville rocks [see below] clearly indicate that it is intrusive in character. Study shows this rock to be a syenite gneiss. It is from fine to medium grained and shows the typical granitoid texture. The weathered surface of all exposures is of a light brown color, while the real color of the fresh rock is greenish gray. Because of the depth of the weathering the fresh rock is usually difficult to obtain. As compared with the other Precam- bric rocks this syenite presents a remarkably uniform structure and composition throughout. Near the contact with the adjacent _syenite-Grenville complex (below described) the rock is usually somewhat finer grained and not so typical in character. Of the two areas mapped, the larger is very irregular in shape and occupies much of the northeastern portion of the district. This mass is mostly heavily wooded and the exposures are often few in number and unsatisfactory. However, many large expos- ures have been found, especially in the vicinity of Northwood, North Wilmurt, Reeds Mill and on the Little Black creek near — the county line. The smaller area lies in the town of Forest- port extending northeastward from Forestport station for several miles and on either side of the railroad. Although much of the area is sand covered, excellent exposures may be seen at Woodhull, Meekerville and in the stream beds southeast, west and southwest - of Anos Siding. The syenite clearly exhibits a gneissic structure although it is not distinctly banded. The concentration of dark colored minerals such as biotite and hornblende along certain lines serves to accentuate the gneissic structure. These lines are wavy and as a rule do not extend far without interruption. All the outcrops show the gneissic structure although it is not always evident in the hand specimen. Under the microscope the mineralogical composition is shown to be feldspar —including anorthoclase, microperthite, and acid plagioclase — quartz, hornblende, biotite, augite, enstatite (or bronzite), magnetite, apatite, zircon, titanite. © : ». z r a ee a i et lS tinh ee ee ee Se pe ee ee \- ee ee Nii tenes yl ete 5 ~ GEOLOGY OF THE REMSEN QUADRANGLE 13 ~The most abundant constitutent is feldspar, which shows a range of from 65 to 80%, while the average amount present is a little over 70%. Of the feldspars, the anorthoclase and the micro- perthite are most common, sometimes the one and sometimes the other predominating. The anorthoclase is recognized by the very minute multiple (microcline) twinning bands, often indistinct but presenting a sort of moiré effect. Occasionally the multiple twin- ning is more distinct and then the feldspar may indeed be micro- cline. Microperthitic intergrowths especially in the larger feldspars are often beautifully shown. Acid plagioclase is a constant con- stitutent of the syenite, though always subordinate in amount. It is mostly oligoclase with low extinction angles although at times some of it ranges over to andesine. The second most abundant mineral is quartz, which makes up from 1o to 25% of the rock or on the average a little over 15%. The quartz grains vary greatly in shape and size and sometimes they are larger than the feldspars. The quartz percentage is often high enough to make the rock a quartz syenite at times approaching granite. The quartz, as well as the feldspar, in nearly all cases appears to have been entirely recrystallized. Among the dark colored minerals hornblende is a very constant constituent. It appears to be common hornblende with its charac- teristic cleavage and pleochroism from light to dark green. Often it may be seen partly or completely changed to chlorite. The maxi- mum amount of hornblende present is about 10 or 12%. Biotite mica is also always present in scattering flakes, never making up more than 5% of the rock. | | The pyroxenes —augite and enstatite (or bronzite) are fre- quently present but always in small quantity. Magnetite — never above 5%-—is a constant constitutent. The development of leucoxene borders around the magnetite may often be seen. A, Many very small prismatic crystals of apatite, generally as in- clusions in feldspar or quartz, occur scattered through the rock. Besides the minerals mentioned occasional small crystals of zircon and titanite are present. All of the dark colored constitu- ents may occur in the same specimen but together they never make up more than 20% of the rock. Syenite-Grenville complex. The rocks here described occupy approximately one half of the Precambric area. Rocks of many different kinds have been included under this head and, both because of the small scale of the map and the scarcity of exposures, it has not been possible to separate these rocks upon the geological map. 14 NEW YORK STATE MUSEUM tin Cia The term ‘‘Syenite-Grenville complex’ is used by the writer because the rocks, for the most part at least, appear to bea rather intricate mixture of the syenitic and Grenville rocks already de- scribed. Especially in certain of the large exposures, as in the vicinity of Forestport, Myers hill, north of Enos, near the northern | limit of the map along the railroad, etc., rocks which if present alone ‘would undoubtedly be classed with the syenite are closely associ- ated with others which show characteristic features of the Gren- ville. The two rocks show great variation in amount although the syenites generally predominate. In large exposures in the field the rocks of the complex may be easily distinguished from the typical Grenville because the bands are not so well developed and straight, and also because of the basic inclusions. They differ from the pure syenite because of a better development of the i structure and a decided lack of homogeneity. There is strong evidence that the Grenville sediments are the © older and that the syenite has been intruded into them. One argument in favor of this view is the fact that the two rocks are so thoroughly involved and that neither may be said to rest upon the’ other. But the strongest argument lies in the fact that portions of the rocks mapped as Grenville may be seen as actual inclusions within the syenite. Among the localities where such inclusions occur are: at the bridge near the mouth of Little Black creek; 2 miles east of Enos on the south side of Ash ridge; near Forestport; _ where the railroad crosses Big Woodhull creek; and to the south - of Myers hill. Thus the syenite appears to be intrusive into and therefore younger than the Grenville. Certain results obtained by C. H. Smyth jrt in the western Adirondacks seem to point to the same conclusion. Because of the great variety of rocks mapped under this heading and the frequent gradations of the different types into each other it is very difficult clearly to describe them. In general it may be said that nearly all of the minerals occurring in either the Gren- ville or the syenite have been found in this complex and also that the microperthite is lacking while the anorthoclase, plagioclase and quartz as well as the dark colored minerals show all sorts of variations in relative abundance. The most common type is a rock of syenitic character, which in the hand specimen very closely resembles the homogeneous syenite. already described. Although under the microscope the rock shows a general lack of microperthite and a greater richness iN. Y. State Mus.” sist An. Reps, v). 2. x 399: wh A din’, atei»_i_ oa a’ rf | (=P ie —~ — er GEOLOGY OF THE REMSEN QUADRANGLE 15 in oligoclase and the dark colored minerals, it is nevertheless thought to be a facies of the homogeneous syenite mass. The dif- _ ference in mineralogical composition just noted might well be explained on the basis of differences in conditions of cooling and crystallization where the molten syenite was so thoroughly in- volved with the Grenville and its associated igneous rocks. Con- tact metamorphic effects must have been common and portions of the Grenville may at times have been absorbed by the molten syenite. Another common type ranges from gray and dark gray to al- most black, the color depending upon the biotite mica content, which is often very high. Other minerals which may be present are anor- thoclase, oligoclase, quartz and smaller amounts of magnetite or hornblende. Rocks of this type usually appear as dark bands within the syenitic masses. } 7 - Other rocks ranging from light to dark color and containing garnets are thought to be Grenville, but they are so closely involved with other masses that they can not be mapped. Such a light colored feldspar rock with large garnets occurs along the railroad about 2 miles northeast of Anos Siding. Another rock generally classed with the Grenville is rich in silli- -Manite and sometimes occurs in the complex as for instance at Forestport. A rock type rich in hornblende and black in color occurs in distinct bands in the complex. A rock of this same character is found in the Grenville and was considered to be an old metamor- phosed gabbro. Besides hornblende the rock contains feldspar ranging from oligoclase to labradorite and a little magnetite. Another rock often present in very irregular masses and ap- parently cutting through all the others is a pegmatite. It is gen- erally coarse grained and not in distinct veins. All sorts of gradations occur between the types here described and these rocks in turn often grade into either the syenite or the Gfenville masses proper. Undetermined Precambric areas. Two areas have been indicated upon the geologic map as Precambric but of unknown character, because the rock masses are completely concealed from view by heavy glacial drift deposits. The area between Forestport and Enos is probably mostly made up of the Syenite-Grenville complex because those rocks bound the area both on the north and on the south. The area between West Canada creek and Little Black creek probably is syenite on the west and Syenite-Grenville on the east. 16 NEW YORK STATE MUSEUM Paleozoic rocks Potsdam sandstone and Beekmantown limestone. The Potsdam sandstone, which is the oldest of the Paleozoic formations bordering the Adirondacks, is certainly nowhere present at the surface within the map limits. There is evidence for believing that this sand- stone is present along the southwestern border of the Adirondacks under cover of later formations. This question has been carefully discussed by Professor Cushing in his report on the Little Falls district.} It is also true of the Beekmantown limestone that no exposures occur: within the map limits. At Little Falls the Beekmantown (Little Falls doiomite) is something like 400 feet thick, but 1t shows a rapid thinning both northward and northwestward. In the vicinity of Cold Brook and Poland, and only a little over a mile from the southern boundary of the Remsen quadrangle, a considerable thick- ness of Beekmantown isshown. Thus, more than likely, 1t extends northward under the younger formations for a short distance at least on the Remsen quadrangle. The Beekmantown comes close to where Black creek enters the map limits, but it seems to have disappeared before that point was reached. There is no evidence whatever to suggest the presence of Beekmantown in the northwestern part of the district. Trenton formation. As here discussed the Trenton formation - ‘includes the Lowville limestone at the base, then possibly the Black River limestones and shales, with the Trenton limestone proper at the top. The Lowville limestone shows in outcrop within the map limits only in the northwest along Black river. The outcrops are in the bed of the river and are well shown a short distance above the mouth of Crystal creek. The rocks are fine grained, compact, of a light bluish gray color and show many of the calcite filled tubes so characteristic of the formation. The layers are generally from 6 inches to a foot thick and constitute a very pure limestone. The exposed thickness of the Lowville here is about ro or 12 feet and although neither the top nor the bottom is visible the maximum _ thickness can not be much over 30 feet. At the mouth of Crystal — creek there is a Precambric outcrop only a few rods from the Low- ville,” and a short distance west Trenton limestone is exposed. 1 Geology of the Vicinity of Little Falls. N. Y. State Mus. Bul. 77. 1905. 2 Along the western border of the Adirondacks the Lowville rests unconformably upon . the Pamelia formation of Cushing. The Pamelia has been traced across the Port Leyden quadrangle by the writer and it is possible that just a trace of it may be present between 7 the Precambric and the Lowville at Crystal creek. fos a” P oS GEOLOGY OF THE REMSEN QUADRANGLE 17 Many outcrops of the Lowville may be seen extending along Black tiver from the locality here described to the type locality at Low- ville. Just below the mouth of Crystal creek some of the limestone layers are clearly ripple marked. From trough to crest the ripples are usually less than an inch in hight, while from crest to crest the distance is only 1 or 2 inches. The Lowville is nowhere exposed in the southern portion of the region, although a few miles off the map limits and between the villages of Newport and Poland, along West Canada creek, a thick- ness of over 20 feet may be seen. The Black River formation of the southwestern Adirondacks consists of a few feet of alternating limestones and shales lying between the Lowville and the Trenton, but not always present. Actual outcrops of the Black River are nowhere visible within the region here described, although the formation is probably present to a greater or less extent under cover of the Trenton proper. A few miles south of the map limits and along West Canada creek, between Newport and Poland, about 7 feet of Black River limestone and shale may be seen resting upon the Lowville. It also occurs at several localities within the Little Falls district. Towards the northwest and a few miles off the map the Black River formation outcrops along Black river. Within the map limits, as above stated, the actual contact between the Lowville and Trenton opposite the mouth of Crystal creek can not be seen because of drift covering. Thus a thin layer of the Black River may possibly be present there. The Trenton limestone proper occupies by far the largest ter- ritory or more than one third the area of the whole quadrangle. With the exception of the small Lowville area above described the Trenton rocks are thought to overlap everywhere upon the Precambric. In general this formation may be said to be made up of thin bedded, dark bluish gray, compact limestones separated by thin shaly layers, except the upper 25 to 35 feet which consists of thicker bedded, gray, coarse crystalline limestones with thin shaly partings. These rocks are everywhere highly fossiliferous, the limestone layers at times being made up almost entirely of ’ shells. The type locality for the Trenton limestone is along West Canada creek, at Trenton Falls, in the southern portion of the region under 1Prosser & Cumings. Sections and Thickness of the Lower Silurian Formations on ae ange Creek and in the Mohawk Valley. N. Y. State Geol., rs5th An. Rep’t. 1898. P. 628-29. 18 NEW YORK STATE MUSEUM discussion. The most complete continuous section of the formation is here shown, which according to Prosser and Cumings has a _ measured thickness of 270 feet with neither top nor bottom ex- — posed. The work of the writer to the west and northwest of Trenton Falls shows that the upper coarse crystalline beds are nowhere much over 35 feet thick and that the Utica shale rests directly upon these beds. Hence the uppermost beds of the Trenton Falls section must be within a few feet of the actual top of the Trenton. The bottom of the Trenton is ae not shown at Trenton Falls, although the dip of the strata and the presence of Beekmantown and Lowville limestone a few miles to the southeast make it appear _ very probable that the lowest beds at Trenton Falls must be close to the bottom. Allowing for the necessary addition to the top and the bottom, the thickness of the complete section at Trenton Falls ~ is at least 280 feet and probably not more than 300 feet. In the section of the Globe Woolen Mills well at Utica the Trenton shows a thickness of 5ro feet, while in the Rome well the thickness is — given as 375 feet. Thus the Trenton shows a greater thickness _ both to the southward and the southwestward. | Because of the importance of the Trenton Falls section a some- what detailed description is here given, although many more details may be found in the writings of Vanuxem,’ Darton,’ T. G. White,® _ Prosser and Cumings,* and Clarke.® For 24 miles between the villages of Prospect and Trenton Falls, West Canada creek has cut a deep narrow gorge through the Trenton limestone. This gorge, with nearly vertical walls, varies in depth from too to about 200 feet and is commonly known as “Trenton chasm.’’ In all there are six waterfalls varying in hight from a few feet to 128 feet. The principal falls are: Sherman fall, about 30 feet high and a short distance above the power house; High falls (¢ mile south of the railroad bridge) consisting of an upper and a lower part with a total fall of 128 feet; the falls at the dam (just north of the railroad bridge) about 40 feet high; and Prospect — ! falls (at the upper end of the gorge) 25 or 30 feet high. According to the topographic map the total drop of the stream within the 24 miles is about 360 feet. At the time of high water especially, the falls present magnificent sights. In spite of the steep slope of the 1 Vanuxem, L. Gcol. N. Y. 3d Dist. 1842. p. 45-56. 2 Darton, N. H. N. Y. State Geol. 13th An. Rep’t. 1894. 1:616—23. 8 White, T. G. N. Y. Acad. Sci. Trans. 1895-96. 15:71-96. 4 Prosser & Cumings. N. Y. State Geol. xsth An. Rep’t. 1898. 1:615—27. UGilerke,\). MoUs. N.Y.) Bde ngs a Bgge) 9 6a—6 7) I a i oe a A ee So er ear Pe oS ee get ne = = = = SESE === + + dUOJSOWIT] UOJUIIT JoMOT “yuUeq Jf] oy} UO 4 ae i UMOYS [JOM OUYAA JO Sq 2UOZ IY, ‘“IIULASIP OY} UT [fey UeUtIOYS ptm ‘pus JOMO] WOl, ,{SMOIIEN ,, 94} JO MOTA 99 GYOAMVYS NOIBNA TIVE «AUR y I 91%Id Plate 2 aye =: i WYNKOOP HALLENBECK CRAWFORD Co. ae re lt oe N. H. Darton, photo. Lower Trenton limestone, Sherman fall, Trenton Falls, Oneida co. = 9UOJSOLUT] UOJUDA 7, 9IPPHAL ‘sjaved toddn puv 19Mo] IY} YOG Surmoys ‘yey ysryy € 21eId GEOLOGY OF THE REMSEN QUADRANGLE 19 stream bed the southward dip of the strata permits an exposure of only 270 feet of the rocks. The lower Trenton limestones are dark bluish gray, thin bedded and fine grained with occasional coarser grained layers inter- stratified. Thin shale partings are nearly always present. On account of the dip the lowest beds are not found at the end of the gorge, but in the “‘Narrows’”’ just above the power house. Accord- ing to Prosser and Cumings' these rocks contain the following fossils: 1 Monticulipora (Prasopora) lyco-- 8 Plectambonites sericeus (Sow.) perdon (Say) HAS GC. 2 Diplograptus amplexicaulis Hall 9 Zygospira recurvirostra Hall 3 Trematis terminalis (Emmons) 10 Bellerophon bilobatus (Sowerby) Hall 11 Asaphus platycephalus Stokes 4 Rafinesquina alternata (Con.), 12 Calymmene callicephala Green = Hall & Clarke C. senaria Con. , 5 Strophomena cf. scofieldi Winch. 13 Ceraurus pleurexanthemus Green -& Schuch. (?) 6 Orthis (Platystrophia) biforata 14 Crinoid segments (Schl.) Bill. 7 O. (Dalmanella) testudinaria Dal. The middle Trenton limestones are mostly dark bluish gray, thin bedded, compact and with pronounced shale partings. According to Prosser and Cumings the middle Trenton fossils include: | t Monticulipora (Prasopora) lyco- 6 Plectambonites sericeus (Sow.) perdon (Say) ECG. 2 Stictopora sp. 7 Tellinomya dubia Hall 3 Rafinesquina deltoidea (Con.) 8 Endoceras proteiforme Hall aes C. g Cyrtoceras sp. 4 Orthis (Platystrophia) biforata 10 Asaphus platycephalus Stokes (Schl.) Bill. 1r Crinoid segments 5 O. (Dalmanella) testudinaria Dal. The upper Trenton limestones are also dark bluish gray, thin bedded, and divided by shaly partings. The more compact strata are frequently interstratified with others which are somewhat crystalline. The upper 26 feet are light gray, coarse grained, crystalline limestones in thick beds which are separated by very thin shale partings. These coarse grained rocks are full of fossil fragments and are best exhibited in the quarries 1 Op. cit. p. 622-23. 20 NEW YORK STATE MUSEUM below Prospect. According to Prosser and Cumings the list of fossils includes: ; t Monticulipora (Prasopora) lyco- 10 Plectambonites sericeus (Sow.) perdon (Say) lake eal CF 2 Escharopora recta Hall 11 Zygospira recurvirostra Hall 3 Trematis terminalis (Emmons) 12 Asaphus platycephalus Stokes Hall 13 Calymmene callicephala Green 4 Rafinesquina alternata (Con.) 14 Ceraurus pleurexanthemus Green GG. 15 Leperditia fabulites Con. 5 R. alternata var. nasuta Con. 16 Endoceras proteiforme Hall 6 R. deltoidea (Con.) H.@ C. ° 17 Orthoceras sp. + Strophomena cf. scofieldi Winch. 18 Bellerophon bilobatus (Sowerby) & Schuch. : 3 19 Dendrocrinus gracilis (Hall) 8 Orthis (Platystrophia) biforata 20 Murchisonia gracilis (Hall) (Schl.) Bill. 21 Stictopora cf. acuta Hall 9 O. (Dalmanella) testudinaria Dal. 22 Crinoid segments Highly contorted strata between undisturbed strata may be seen between the lower and upper portion of High fall, and also along the footpath especially opposite the crest of High falls. These ~ phenomena will be discussed later under a separate heading. - : Another Trenton section ranking next in importance to the one just described is that at Gravesville and extending from the village for more than a mile up Mill creek. A thickness of nearly 200 i is here shown with neither top nor bottom exposed. ee a At Grant and extending for a lialf mile down Black creek agood section (20 to 30 eee of lower to middle Trenton beds ee seen. The upper Trenton limestones are well shown at Hinckley; be- tween Trenton and Holland Patent; north and northeast of Steuben Valley; along Town Line (Cincinnati) creek from Prospect station — (R. W. & O.) to Remsen; in the vicinity of Honnedaga and Bard=—" well Mill; and south of Alder Creek station. Besides these many _ smaller outcrops were found. : ae The upper, gray, coarse crystalline beds form the surface rock (largely covered by glacial drift) over most of the western portion of the Trenton limestone area. They are especially well shown near the Utica shale contact line. St Dolgeville (upper Trenton) shales. A series of alternating thin’ bedded limestones and shales, lying between the Trenton proper and: % the Utica shale, and found in the Little Falls district is called by Cushing the Trenton-Utica Passage Series.1 Recently, however, Cushing has proposed the name Dolgeville (upper Trenton) shales 1 Op. cit. p. 31-32. Ly ve es % N. H. Darton, photo. Upper gorge, Trenton Falls, Oneida co. Upper Trenton limestone . SuUOJSOUT] UOJUOIT s9ddyqQ ‘HS oy} Jo yavd soddn oy} ut UMOoYsS st d9uU0}sSoUTT] OUT][VISAID DAISSLUL OY T, ‘aSplIq pvol[IeyY Yorpuosipy oy} sAoqe Yoo1d vpvury jso9A\ JO apis jsvo ay} uO HUD — ¢ GEOLOGY OF THE REMSEN QUADRANGLE 21 for these beds.t These rocks are absent from the Trenton Falls region except probably to a small extent in the extreme southeastern portion. They are mapped as occupying the extreme northwestern corner of the Little Falls quadrangle and hence would extend over, to a greater or less extent, upon the Remsen quadrangle. It is highly probable that these rocks are thus present although outcrops are nowhere shown because this region is sodeeply covered by glacial drift as to completely conceal all underlying formations. The rocks of this series are transitional in character, the limestone layers being very similar to the Trenton while the shale layers are very similar to the Utica shale. The Utica shale formation. The Utica shale, wherever present, rests directly upon the coarse crystalline beds of the upper Trenton. From the lithologic standpoint the formation is remarkably uniform and free from limestone or sandstone beds. The shale is black, thin bedded to even laminated, and because of its hardness and easy splitting is often popularly miscalled ‘“‘slate.’’ As seen upon the geologic map the shale is entirely confined to the western part of the quadrangle where it occupies most 3 the area west of the R. W. & O. Railroad. The contact between the shales and the upper, coarse grained beds of the Trenton is a very sharp one although the lowermost beds of shale are more or less calcareous, thus showing that the change from limestone to shale is not so abrupt as the outward appearance of the rocks seems to indicate. The two formations may be seen in close proximity at several places along the stream beds to the north and northeast of Steuben Valley. Perhaps the best locality for observing the contact is along the railroad (R. W. & O.) about # of a mile north of East Steuben station, where the shale and the coarse grained limestone are within 1 or 2 feet of each other. Beyond the map limits to the south, the sharp contact is well shown in the bed of Nine Mile creek, 14 miles southeast of Holland Patent. A low anticline here brings up the upper Trenton lime- stone with Utica shale resting on either limb. The typical Utica shale beds extend well up on the sides of Starr hill where they reach an elevation of about 1560 feet. The lowest shale beds east of Starr hill lie at about 1250 feet. Hence the thick- ness of the Utica shale here must be something over 300 feet. A 1 Since the appearance of the Little Falls report it has become evident that this: fore ation therein mapped as ‘‘ Trenton- Utica passage beds ”’ is in reality a shaly eastern representative of the upper Trenton limestone of the type section, as I suggested at the time N. Y. State Mus. Bul. 77, p. 63-64]. It seems also that this division is separable from the Trenton and Utica asa lithologic unit throughout the Mohawk valley. For this shaly phase of the upper Trenton I propose the name of Dolgeville shale, the full thickness with both contacts being exposed in the banks of East Canada creek just below Dolgeville. [Signed] H. P. CUSHING 22 NEW YORK STATE MUSEUM thickness of approximately 600 feet in the southern part of the Little Falls district is given by Cushing. The record of the Camp- bell well near Utica shows 710 feet of the shale there. The deep well at Rome shows a thickness of only 300 feet of shale. Thus there seems to be a notable thinning of the Utica shale in passing northwestward. Lorraine beds. The Lorraine beds of the Hudson River group appear at only one place within the map limits, namely at the top of Starr hill. The beds there show a thickness of about 200 feet with the top not reached. As is usually the case in central New York these lower beds appear to be destitute of fossils. Penn mountain and other high hills just west of the Remsen quadrangle are capped by the same formation. There is no sharp line of demarcation between the Utica and — the Lorraine and thus an exact boundry line can not be drawn. Passing upward the Utica black shales give way to generally lighter colored, rather more sandy shales containing frequent thin beds of gray sandstone. At times, however, the Lorraine shales closely resemble the Utica shales. Good exposures may be seen on the western side of Starr hill and also near the top of Penn mountain at about the 1700 foot level. STRUCTURAL FEATURES Folds The Paleozoic formations show a very perceptible southwest- erly dip but it is by no means uniform. “For instance to the north of Remsen and in the vicinity of Honnedaga the limestone beds show very little departure from horizontality, while to the north of Steuben Valley they show a dip of approximately roo feet per mile to the southwestward. Again in the bed of Mill creek, about a mile above Gravesville, the limestones show a very sharp dip of 15° to the southwest. In other cases the southwestward dip is just enough to be noticeable in the outcrops. Thus we see that strata which in a given locality lie almost horizontal may within a short distance show a comparatively steep dip giving rise to low folds whose axes extend northwest and southeast. Another set of folds whose axes extend northeast and southwest are also more or less clearly distinguishable. Such are the folds accompanying the Trenton fault and fold (below described). A low anticlinal fold with similar strike has been observed to the _ northeast of Steuben Valley where along one stream the limestone a tthe Ng ns a Ag ¢ Se the Dolgeville fault and the branch of the Little Falls fault. GEOLOGY OF THE REMSEN QUADRANGLE 23 clearly dips to the west while along another stream a mile east the dip is southeastward. In the stream bed below Grant the limestone clearly dips northwestward thus suggesting the limb of a similar. fold there. Off the map limits, about 2 miles southeast of Holland Patent and in the bed of Nine Mile creek, a very distinct anticline with northeast-southwest strike is exposed. The upper Trenton is here brought to view with shale dipping away on either side. Aside from these larger folds numerous small ones occur, as for example in the bed of West Canada creek.at Trenton Falls village. Faults Trenton fault and fold. A line of distinct faulting and folding passes from near Prospect village for 9 miles southwestward to a ica. bt Trenton. 100 Feet. Fig. 1 Section across the line of sharp folding 24 miles south- west of the village of Trenton. The minor faulting is not shown in the drawing. Stittville beyond the map limits. The line of disturbance is almost straight and beginning east of Prospect, it passes near Prospect station (R. W. & O. R. R.), just west of Trenton, thence off the map through Holland Patent and to Stittville. That portion of the line between Trenton and Holland Patent has been very briefly described by Darton,’ but the more important part lying between Trenton and Prospect is here described for the first time. The writer has called the whole line.of disturbance the Trenton fault because it passes through the town of Trenton. The Trenton fault is of interest for several reasons: because it is the most westerly of all the series of Mohawk valley faults yet described; because it is the only one of the series which shows thrust faulting ; and because it is one of a very few which have the downthrow side on the west. Two other faults of the series having downthrow on the west are KIN. Y. State Geol. r4th An. Rep’t. 1895. p. 52-53. 24 NEW YORK STATE -MUSEUM Between Trenton and Holland Patent the disturbance has manifested itself chiefly as a sharp anticlinal fold with a steep western front accompanied by comparatively slight faulting. The above figure shows the condition of things here poe to the writer’s conception. According to Darton! normal faulting has been the principal cause of the displacement and as a result of slipping, the Utica shales, on the downthrow side, have been bent upward while the limestone beds on the upthrow side have been bent downward. According to him the upper Trenton has been sharply faulted against the Utica, the amount of displacement being possibly as much as 60 feet. A careful study of the limestone-shale contact has failed to reveal any such sharp or extensive faulting as sug- gested by Darton. According to the writer the steep dips of the limestone and shale are due entirely to the development of an anti- cline whose western limb is very steep and sometimes nearly ver- tical so that it approaches the overturned type. As a result of the folding and later removal of shale by erosion the limestone beds do appear displaced or raised above the level of the shale The difference in level is often 40 to 60 feet as Darton suggests but it is not due chiefly to faulting. ; - If the lateral pressure which formed the anticline had continued, a typical overturned fold and finally a thrust fault would have de- veloped. As it is, the only evidence of faulting is within the body of the limestone itself, near the shale contact, where small thrust — faulting may occasionally be seen. All along the line between Hol- land Patent and Trenton the harder, more resistant limestone beds stand out as a low sharp ridge while the softer shales on the west have been worn down. In the vicinity of Prospect station 14 miles southwest of Prospect there is also abundant evidence of disturbance. Here, however, upper Trenton limestones only are present. Along the small streams just north of the station they are seen to be strongly folded, in one case the limestone beds standing in ver- tical position. Also to the west of the station in the bed of Cin- cinnati (Town Line) creek the limestone beds are much disturbed by folding. In this vicinity some minor faulting has been noted although for most part the disturbance shows itself in the folding. ~ Between Prospect station and Prospect village the country is. deeply drift-covered, while at Prospect occurs the principal dis- turbance visible along the line. A thrust fault of considerable Be Op. cit. p. 52-53. Siet3 ~~ tee F Oe ee ae ag Ot waee * x - - ~ - — = W. J. Miller, photo. Looking westward and parallel to the strike of the fault at Prospect. On the right are thick beds of the upper Trenton; on the left are highly in- clined, thin bedded middle Trenton strata; while between are broken and crushed middle Trenton rocks. The water’s edge on the right lies along the fault plane. - Sd 4, + % ae a GEOLOGY OF THE REMSEN QUADRANGLE 25 throw is clearly exhibited in the creek bottom between Prospect falls and the highway bridge. The topographic map is here not accurate in detail and the following sketch map will give a better idea regarding the location of the fault. Before reaching the falls the stream flows due west and at the falls makes a sharp turn to flow about 200 yards east-southeast till the fault line is struck. At the latter point another sharp turn is Fig. 2 Sketch map showing the course of West Canada creek and the position of the fault near the village of Prospect made so that the stream flows west-southwest for 50 or 60 yards, and parallel to the fault line. Then the course of the stream is due south to the highway bridge. Where the creek flows parallel to the fault line the fault plane is clearly exposed and in reality forms the north bank of the creek [see pl. 6 and 7]. The strike of the fault is n. 70° e. and the dip of the fault plane is 55° to the south. It is a thrust fault with. the downthrow side on the north [see fig. 3]. The rocks on the downthrow side are the thick bedded, coarse crystalline limestones belonging at the summit of the Tren- ton formation. These rocks form a bold rocky point extending 26 NEW YORK STATE MUSEUM eastward to the creek and they show variable dips of from 5° to 15° a little to the south of west. The rocks in the creek bed on the upthrow side of the fault are middle Trenton limestones. A short distance away from the fault plane these rocks are highly inclined showing a uniform maximum dip of 35° a little to the east of south. Continuing southward to the bridge higher and higher Trenton strata are seen and the dip gradually diminishes to 12°. Below the bridge the dip continues to decrease until finally at about 150 yards the strata lie in a horizontal position and the coarse lime- stone of the uppermost Trenton is visible at the top of the gorge. Still farther southward the rocks dip northward at a low angle. In the immediate vicinity of the fault and on the upthrow side the rocks are highly crushed and folded. This crushed zone is Fig. 3 Section showing the condition of things at the fault near Prospect. Looking south- - west and parallel to the fault plane about 40 feet wide [see fig. 3]. The rocks on the downthrow side are not crushed and the fault plane is shown as a smooth clean break [see pl. 7]. Along the fault plane slickensides are common and also fault breccia made up of limestone fragments which have often been recemented by white coarse crystalline calcite. On both sides of the main fault plane there are a number of fault slips of very small throw which represent minor fracturing in the immediate vicinity of the main fault. Except for a slight south- westward dip the strata at Prospect falls show no sign of disturb- ance. Because of the existence of the wide crushed zone on the upthrow side the character of the folding in that zone can not be determined. Hence the exact throw of the fault can not be given although it can be fairly well approximated. Asa result of the faulting the beds of the middle Trenton have been brought up to the level of the coarse crystalline beds of the upper Trenton and hence the fault must be of the thrust or reversed type. A measurement by the W. J. Miller, photo. Looking north upon the fault plane at Prospect. Except at the extreme left, the whole rock surface shown is that of the fault plane itself. The dark streak near the left margin and nearly under the small dead tree represents the contact between the crushed middle Trenton and the heavy bedded upper Trenton. —, ’ 4 ¢ ” , * GEOLOGY OF THE REMSEN QUADRANGLE 27 writer of the thickness of the upturned strata from the base of the coarse crystalline beds to the crushed zone at the creek level near the fault plane gave 140 feet. This result corresponds to within a few feet of the thickness obtained by Prosser and Cumings for the same set of strata farther down the gorge. According to those - authors the conspicuously contorted stratum opposite the top of the lower fall of High fall occurs just above their zone A® or 144 feet below the top of the Trenton. This same contorted stratum has been traced by the writer to near the fault and between it and the fault there intervenes a thickness of 25 or 30 feet of still lower strata. It is evident therefore that the beds as low at least as the upper part of Prosser and Cumings zone A’® are thrown by faulting against the gray crystalline upper Trenton beds. Thus the strati- graphic throw of the fault (disregarding the crushed zone) is some- thing like 140 feet. The throw or vertical displacement is prob- ably from 30 to 50 feet greater than the stratigraphic throw. Be- cause of the high angle of dip of the fault plane the heave (hori- zontal displacement) must be considerably less than the throw. Upturned strata are often present among the shales on the downthrow sides of the Mohawk valley faults. They are due to an updragging effect produced by normal faulting. At the Trenton fault, however, the sttata are upturned on the upthrow side and were bent upward by the lateral pressure which first probably de- veloped a fold and later a fracture so that the middle Trenton rocks were pushed upon the upper Trenton. Where the fault line would be expected to cross the creek about 4 of a mile eastward the only sign of disturbance is a small but very distinct fold in the limestone beds. Thus the fault above described dies out so rapidly that within the } mile it is entirely gone and passes into a small fold. Beyond this the line of dis- turbance can not be traced because of heavy drift deposits. Minor faults. A number of small faults have been noted along the gorge between High fall and Prospect but the throw is always slight. The Trenton rocks have been considerably disturbed by folding and faulting on Mill creek and one of its tributaries about a mile above Gravesville. Sharp folding is well shown where the line crosses Mill creek (at the mill), while folding accompanied by faulting of unknown though small extent is exhibited where the line crosses the tributary (the second one above Gravesville) a quarter of a mile above its mouth. This line of disturbance strikes n. 70° w. and it can not be traced across country. 28 NEW YORK STATE MUSEUM Dip of the Paleozoic formations As the Paleozoic rocks were originally laid down nearly hor- izontally movements since their deposition have caused them to have a general southwestward dip. The amount of the dip is usually small and may be clearly demonstrated by comparing the altitude of given horizons within the Trenton at different places. At Trenton Falls the top of the Trenton limestone is 1100 feet above sea level, while the same horizon was struck at 142 feet below sea level in the Globe Woolen Mill well at Utica. ‘Thus the differ- ence in elevation of the same horizon between these points 14 miles apart is 1242 feet, showing a southward dip of go feet per mile. Again, the top of the Trenton 1 mile south of Alder Creek sta- tion is at 1280 feet, while the same horizon in the Rome well is 205 feet below sea level. The difference in elevation is 1485 feet and the distance is 18 miles, which shows a dip of 82 feet per mile for the limestone. At Grant, lower Trenton is exposed at 1200 feet, while at Graves- ville 5 miles to the southwest the same beds lie at goo feet, thus giving a dip of 60 feet per mile. The difference in elevation between the top of the Trenton at Bardwell Mill and Remsen, which places are 44 miles apart is ap- proximately 4o feet, thus giving a dip of 9 feet per mile. Over the western part of the town of Remsen the strata must lie almost horizontal as shown by the outcrop of the upper Trenton over such an area at practically the same elevation. Uppermost Trenton beds are shown at Remsen and also at a point 14 miles northeast of Steuben valley. The distance between these points is 24 miles and the difference in elevation is about 250 feet, so that here the southwestward dip is about too feet per mile. Certain marked variations from this general southwestward dip due to the development of the Trenton fault and fold have already been described. Joints The Precambric rocks are everywhere highly jointed and the joint planes are always vertical or at high angles. After many ob- servations the writer has not been able to make out any well defined system. Even over short distances the directions are very variable. Locally, however, two well developed joints may gen- erally be seen crossing each other at rather high angles. Besides these other minor and irregular joints are present. The Paleozoic rocks, too, are thoroughly jointed and, as in the case Of the Precambric rocks, these joints are mostly nearly verti- GEOLOGY OF THE REMSEN QUADRANGLE 29 cal. Although these joints show great variation in direction and degree of development, nevertheless over most of the Paleozoic area two sets running approximately east-west and north-south appear to predominate. These are particularly well seen in the vicinity of Trenton Falls and Remsen. The vertical walls of the gorge at Trenton Falls are principally due to the breaking away of large limestone masses along the north-south joint planes. The east- west joints may here be seen extending across the stream at many places, but especially at the falls themselves. The falls are all due to the existence of the joints since when a large mass of limestone is removed a vertical wall is left over which the water falls. Thus the falls retreat and reform by the removal of joint blocks as, for example, in the case of Sherman fall. Here at high water the water falls over one joint plane on the eastern side and over an- other a number of feet back on the west side. When the water is low it all passes over the rear joint on the west [see pl. 2]. It is very evident that, in the course of time, the whole block of lime- stone left between the two joints will be removed. In the bed of Cincinnati (Town Line) creek, from 1 to 14 miles below Remsen an interesting drainage feature is due to the joint _ planes in the coarse crystalline (upper Trenton) limestones. Sev- eral hundred yards above the bridge, at time of low water, the stream disappears entirely through the joints and after a subter- ranean course, mostly along the joints, it reappears near the bridge. Foliated structure A foliated or gneissic structure is highly characteristic of all the Precambric rocks. It is exhibited best of all in the ancient Gren- ville sediments, next best in the rocks of the Syenite-Grenville com- plex, and least in the pure syenite. The excessive foliation of the Grenville is accentuated by the alternating light and dark bands above described. The foliation of the syenite though distinct is brought out only by the dark, narrow, irregular, wavy streaks passing through the otherwise homogeneous rock mass. As a result of many readings it may be stated that the Pre- cambric foliation planes all show a strike varying between n. 60° e. and n. 80° e. This result agrees closely with that obtained by Cushing for the Little Falls quadrangle and for the Long Lake quadrangle of the mid-Adirondacks. The dip of the foliation _ planes is sometimes north and sometimes south but nearly always at very high angles. Often the Grenville and the Syenite- Grenville complex rocks are locally highly plicated or crumpled 30 NEW YORK STATE MUSEUM It is interesting to note that the strike of the Trenton fault and fold, as well as the strike of a number of low folds within the region corresponds closely to the strike of the Precambric foliation planes. This shows that the pressures so different in intensity, and which produced both sets of phenomena so widely separated in time, acted in the same direction. . Contorted strata within the Trenton !- 3A é ae Excellent examples of highly folded or contorted strata between nonfolded strata may be seen along the sides of the gorge at Tren- ton Falls. Dr J. M. Clarke has called the writer's attention to a similar case of interbedded contorted limestones described by Sir Feet. Fig. 4 Highly folded and broken strata between nonfolded strata as seen along the footpath opposite the crest of High falls. Drawn from nature William Logan? and occurring on the Forillon peninsula of Gaspé, along the Gulf of St Lawrence. According to Clarke? these con- tortions lie in the Cape Bon Ami beds of the lower Devonic. At Trenton Falls the folded beds lie at two distinct horizons within the Trenton limestone. According to Prosser and Cumings?*. who have made careful measurements of the thickness of the lime- stone at this locality, the base of the lower contorted zone lies 144 feet below the top of the Trenton. This zone is from 4 to 6 feet thick and is visible only at the crest of the lower part of High fall and in the upper end of the gorge near Prospect where the strata are highly inclined [see pl. 8]. Using the measurements of Prosser and Cumings the base of upper folded zone lies about 65 or 70 feet 1 See paper by the writer in Jour. Geol. 1908. 16:428-33. 2 Geol. Can. 1863. p. 391-92. 3N. Y. Mus. Mem. 9. 4N. Y. State Geol. rsth An. Rep’t, p. 615-27. Plate 8 T. G. White, photo. The lower contorted and broken zone as seen near the crest of the lower ~‘rt meertienetall (From N: Y. Acad. Sci: Trans. v. 15,, pl. III, fig: A) & ET GEOLOGY OF THE REMSEN QUADRANGLE ~~. 31 below the top of the Trenton. This zone varies from about 8 to 15 feet in thickness and is well shown along the path opposite High fall. From this point it may be traced along the sides of the gorge for nearly 2 miles to Prospect village. The impure limestone layers of both the folded and the non- folded portions average only a few inches in thickness and are separated by thin shale bands. Within the folded zones the layers are, in rare instances, scarcely folded or broken; sometimes they are gently folded; most commonly they are highly folded or con- torted ; while occasionally some of the layers are broken and pushed or faulted over others. Numerous observations show the strike of the folds to be from n. 50° e. to n. 65° e. or practically parallel to the strike of the Trenton fault and also parallel to the very low folds of the Trenton limestone in this region. It should be noted that these contorted strata occur ce in a very local district. As far as can be ascertained they are visible only in the Trenton Falls gorge and in the bed of Cincinnati creek, 1% miles southwest of Prospect. Along Mill creek, above Graves- ville, the contorted strata do not show in the excellent Trenton’ section there exposed. Cause of the folding. Vanuxem! states that the folded layers are more thoroughly crystalline than the layers above and below and that as the material of the disturbed layers was being crystal- lized it caused an expansion which manifested itself laterally by throwing the layers into folds. However a careful study has failed to show any real difference in degree of crystallization and even if such difference could be found it is difficult to see how simple crystallization could bring about such a considerable expansion. T. G. White? cites Prof. W. O. Crosby as suggesting that the folds may have been caused by the great weight of overlying strata. But this does not explain the sharp and even overturned folds and minor thrust faults which imply a distinct shortening of the layers within the folded zones. In some places the structure greatly simulates cross-bedding. White* gives photographs showing supposed overlap structuré and channel filling. Since these structures are associated in the same zone, with truly folded and broken strata some other ex- planation must be sought. ' 1Geol. N. Y. 3d Dist. 1842, p. 90. _ 3N. Y. Acad. Sci. Trans. 15:89-g0. Li. Op. cit. pl. 3, fig. B and pl. 4, fig. B. 32 NEW YORK STATE MUSEUM It has occurred to the writer that the cause may have been a lateral compression which caused most of the limestone beds ta become denser without being folded, while certain other layers yielded by folding. This would seem to imply a greater rigidity for the folded zones, but if anything the evidence points to less rigidity. ? Regarding the Canadian occurrence above referred to Logan says: “Tt would appear as if the layers after their deposit had been con- torted by lateral pressure, the underlying stratum remaining un- disturbed, and had then been worn smooth before the deposition of the next bed. Where the inverted arches of the flexures occur some of the lower layers are occasionally wanting, as if the corru- gated bed had been worn on the under as well as the upper side.’” But it is difficult to see how such a lateral pressure could cause certain layers to become highly folded and broken while the layers immediately below them are undisturbed. Also the apparently worn character of the upper and lower sides, mentioned by Logan and which is likewise true of the Trenton Falls occurrence, is left without explanation. It is thought that the folded structure at Trenton Falls was, in reality, caused by a differential movement within the mass of the Trenton limestone. That the whole body of the limestone has been moved is clearly demonstrated by the existence of the thrust fault at Prospect. It is easy to see how when the force of com- pression was brought to bear in the region there would be a tend- ency for the upper Trenton beds on the upthrow side to move more easily and consequently faster than the lower Trenton beds. For instance the portion A in figure 4 being separated from C by an intermediate mass B of slightly less rigidity, would slide over C and cause the portion B to become ruffled or folded. Occasion- ally parts of B would become fractured or faulted. A similar explanation would also apply to the lower folded zone. The folded zones thus merely indicate horizons of weakness along which the differential movement has taken place. As thus explained it is evident why the strike of the minor folds, the strike of the fault, and the strike of the large low folds of the region should all be parallel and why the contorted strata should be so local in occurrence, because all these phenomena were pro- duced by the same local pressure. The differential movement would also readily account for the rubbed or worn character of the upper and lower sides of the contorted zone. It is interesting to note that similar phenomena of contorted between nonfolded strata have been observed in clay banks of GEOLOGY OF THE REMSEN QUADRANGLE 33 Pleistocene age along Black river to the north of Trenton Falls and also along the Canal feeder west of Forestport. The latter occurrence has been described and figured by Vanuxem.' Regard- ing this phenomenon Vanuxem says: ‘‘ No cause can reasonably be assigned but different degrees of lateral pressure.’’ The folding is often so great, however, that the required differences in degree of lateral pressure are altogether too great. The writer believes that, in principle, the explanation given for the contorted limestones may apply here also, except in the case of the clay beds the move- ment of upper over lower masses may have been caused by ice ac- tion or by having been pulled down the hillside by gravity. Or as Salisbury and Atwood? have suggested for such a phenomenon in Pleistocene clay, that the cause may have been lake ice or ‘‘ the grounding of an iceberg on the surface before the overlying layers were deposited.’’ In any case the cause of the movement in these superficial clays is very different from that of the ancient Trenton limestones. Stich interbedded contortions are very common in the Pleistocene clays of New York, especially along the Hudson river valley. THE PALEOZOIC OVERLAP As already stated the Paleozoic rocks overlap upon the Pre- cambric. This was caused by a gradual sinking of the Adirondack region while Paleozoic deposition was going on, so that the younger formations encroached farther and farther upon the sinking land mass. Since the Potsdam sandstone nowhere outcrops along the south- western border of the Adirondacks, any evidence for its presence as the lowermost of these overlapping formations must be sought for in deep well sections. This question has been clearly dis- cussed by Professor Cushing who uses data furnished by both Prosser and Orton. The writer here merely wishes to state the general conclusion that in the Ilion, Utica and Rome wells the presence of Potsdam sandstone has not been definitely proved because of the difficulty in distinguishing Beekmantown and Potsdam on the one hand and Potsdam and Precambric on the other. Farther northward in certain Oswego county wells the presence of the Potsdam has been demonstrated. Since the Potsdam does not outcrop along the Precambric boundary line east of these wells it is evident that younger formations overlap it upon the Pre- cambric. j — 1 Op. cit. p. 214-15. 2 Jour. Geol. sg yep 8 Geology of the Vicinity of Little Falls. N.Y. State Mus, Bul. 77. 1905. p. 51-56. 34 NEW YORK STATE MUSEUM Although the Beekmantown is not exposed within the map limits there is no question regarding its presence as an overlapping formation. In the northwest corner of the quadrangle, along Black river, the Lowville and Precambric are so close together as to preclude the presence of Beekmantown. Near the south boundary at Cold brook, the Beekmantown is exposed and doubt- less extends northward under the Trenton. In the wells to the south and southwest at and near Utica and at Rome, the Beekman- town is present showing a thickness which is not accurately known, but which is quite certainly at least several hundred feet. Passing northwestward from these wells to the Precambric boundary the Beekmantown shows a diminution in thickness from several © hundred feet to nothing, which is just what would be expected in the case of overlap. Ag=Grenville, Sy=Syenite. Sya= Grenville—Syenite. St= Trenton, Sh=utica—Lorraine, Horiz. scale: Kinch=1mile. Vert. Scale:1inch=2400feet. Fig. 5 Structural section across the region peeing from Starr -hill east-northeast and through — sh ridge ; Within the map limits the Trenton formation, so far as can be determined, everywhere rests upon the Precambric, along the Pre- cambric boundary. Along Black river, in the northwestern part of the quadrangle, the Lowville may be seen practically in contact with the Precambric. Thus the facts clearly show that the Trenton overlaps the Beekmantown upon the Precambric. | The Trenton shows a thickness of 510 feet in the Globe Woolen Mill well at Utica, 575 feet in the Chittenango well, and 435 feet (including the Lowville) in the Rome well. Within the Remsen quadrangle the maximum thickness of the Trenton including the Lowville is about 300 feet. Along the Precambric boundary there is strong evidence to show that the thickness of the Trenton is much less. Such evidence may be found along the line between Bardwell Mill, where upper Trenton is shown, and the mouth of Little Black creek where Precambric outcrops. When the differ- ence in elevation and the greatest possible slope of the Precambric surface between these points are considered, it is evident that no a: ee P j 7 oS ee oer GEOLOGY OF THE REMSEN QUADRANGLE 35 * such thickness as 300 feet of limestone can here be present. In other words a well starting at the top of the Trenton at Bardwell _ Mill would strike the Precambric much short of 300 feet. “ 20: Hinckley, 20, 42, 43, 45, 40. Holland Patent, 20, 23, 24, 46, 47. Honnedaga, 20, 22. Hornblende, 10, 11, 12; 43, 15. Hypersthene, 11. Ice erosion, 40. Ice movement, direction of, 40-41. Ilion, 33. Iron ore, 48. Joints, 28-29. Kame-morainic deposits, 42-43. Labradorite, 11, 15, 48. Leperditia fabulites, 20. Little, Black creek; ior2. 114 ans a 37: Little Falls, 16, 30. Fittle. Falls.- district, 37,: 422 time stone boulders, 10; type section, 38. Little Falls dolomite, 16. Little Falls fault, 23. Little Falls quadrangle, 29. Little Woodhull creek, o. Logan, Sir William, cited, 30, 32. Long Lake quadrangle, 29. Lorraine beds, 22; thickness, 22. Lowville limestones, 7, 16, 17, 34, 30; thickness, 16; building stone, 47. Lowville shales, 38. Magnetite, 11, 12, 13, 15, 48. Meekerville, 12, 47. Mica, see Biotite mica. Microcline, 13. ’ Plagioclase, 11, STATE’ MUSEUM Microperthite, 12, 13, 14. Middleville, 46. Mill creek, 20, 22, 27; 34: Mohawk valley, 41. Monticulipora (Prasopora) lycoper- don, 19, 20. Murchisonia gracilis, 20. - Myers hill, 14, 35-36, 44. Newland, D. H., cited, -1o. Newport, 17. Nine Mile creek, 21, 23, e North Wilmurt, 12. Northwood, 12, 36, 37, 43. Oligoclase, 11, Oriskany, 46. Orthis (Platystrophia) biforata, 19, 20. (Dalmanella) testudinaria, 19, 20. Orthoceras sp., 20. Orton, Edward, cited, -33. Oswego county, 33. 13, 15, 48. Paleozoic rocks, 16-22; Precambric, 33-35. Pamelia formation, 16. Pesimatite,” 15: Penn mountain, 22. 12, “33, tee Platystrophia biforata, see Orthis (Platystrophia) biforata. Plectambonites sericeus, 19, 20. Poland, 16, 17, 46. Port Leyden district, 42. Port Leyden quadrangle, 16. Potsdam sandstone, 7, 16, 33. Prasopora lycoperdon, see Monticu- lipora (Prasopora) lycoperdon. Precambic rocks, 9-15; undetermined areas, 955. Precambric surface, 35-37. Prospect, 20, 23, 24, 30; 31, 32, 40a 45, 46, 47; fault near, 26. Prospect falls, 25. Prosser, C. S., cited; 47, “18a 27, 30; 33. Pyrite, 11. overlap on Quartz, 10, 11, 12, 13, 14, 15, 48. =x = Pe INDEX TO GEOLOGY OF THE REMSEN QUADRANGLE 51 Rafinesquina ailternata, 19, 20. var. nasuta, 20. deltoidea, 19, 20. Reeds Mill, 12, 37, 4i. . Remsen, 20, 22, 28, 20, 41, 42, 43, 45, 46, 47. Road metal, 47-48. Rome, 18, 22, 28, 33, 34, 306. Salisbury, R. D., cited, 33. Salisbury iron mine, 48. Sand, 44-45, 48. Sand hill, 37, 43. Sherman fall, 29. Sillimanite, II, I5. Smyth, C. H. jr., cited, Io, 14. Soils, 46-47. : rate fall, 8, 21, 22, 34, 40, 41, 45. Steuben, 46. Steuben valley, 20, 21, 22, 28, 42, 47. * Stictopora sp., 19. cy. acuta, 20. Stittville, 23, 46. Strophomena cf. scofieldi, 19, 20. Structural features, 22-33. Syenite, 13; foliated structure, 29. Syenite gneiss, 12-13. Syenite-Grenville comp!ex, foliated structure, 29. 13715; Tellinomya dubia, 109. Till, 41-42. Titanite, 12, 13. Topography, 8-9. Town Line creek, 9, 20, 24, 20, 46. Trematis terminalis, 19, 20. Trenton, 20, 24, 42, 46, 47. ‘Trenton Falls, 17, 18, 23, 28, 20, 30, 32, 33 35, 38, 39, 43, 44, 45, 46. Trenton Falls district, description, 18; type section, 38. Trenton Falls gorge, 31. Trenton formation, 16-20, 34; thickness, 34, 36. Trenton limestones, 7, 17-20, 38, 42; thickness, 18, 20; fault and fold, 23-27; dip, 28; joint planes, 29; contorted strata within, 30-33; slope of surface upon which it was being deposited, 36; building stone, 47; road material, 48. Trenton-Utica passage series, 20, 21, 37: Utica, 18, 22, 28, 33, 34, 36. Utica shales, 7, 21-22, 38; thickness, Ze: Vanuxem, Lardner, cited, 18, 31, 33. Vernon, 36. West Canada creek, 8, 9, 15, 17, 18, 23, 43, 44, 45, 46, 47, 48; sketch map showing course of, 25. White, T. G., cited, 18, 31. Wilmurt sheet, limestone, Io. Woodhull, 12. ZiCon,-1y, 12° 13: Zygospira recurvirostra, 19, 20. New York State Education Department New York State Museum Joun M. Crarxe, Director PUBLICATIONS Packages will be sent prepaid except when distance or weight renders the Same impracticable. On 10 or more copies of any one publication 20% discount will be given. Editions printed are only large enough to meet special claims and probable sales. 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Director’s report for 1907 Botany Economic Geology Entomology Archeology Geology ' Bulletins are also found with the annual reports of the museum as follows: 1 Zoology 43 2 Botany 44 3 Economic Geology 45 4 Mineralogy 46 5 Entomology 47 6 “ 48 7 Economic Geology 49 8 Botany 50 9 Zoology 51 10 Economic Geology 52 Tt “ 53 12 54 13 Entomology 55 14 Geology 56 15 Economic Geology 57 16 Archeology 58 17 Economic Geology 59 18 Archeology 60 19 Geology 61 20 Entomology 62 21 Geology 63 22 Archeology 64 23 Entomology 65 24 o 66 25 Botany 67 26 Entomology 68 27 ss 69 28 Botany 70 29 Zoology : 71 30 Economic Geology 72 31 Entomology 73 32 Archeology 74 33 Zoology 75 34 Paleontology 76 35 Economic Geology “Eh 36 Entomology 78 37 a 79 38 Zoology 80 39 Paleontology 81 40 Zoology 82 ‘41 Archeology 83 42 Paleontology 84 Bulletin Report Bulletin Yr2-15 48, Vv. 1 64 56, RO sts b0;) Vat 65 56, TS, LO blast 66,67 56, 20-25 52, Vv. 1 68 Os 26-31 53, V.1 69 56, 39-34. 54, Veok 70, 71 57, 35,36 54,Vv.2 72 57s 37-44 54, V..2 73 7s 45-48 54,Vv.4 74 57) 49-54 55,V.1 7/5 57> 55 56,Vv. 4 76 57, 56 66,912 77 575 57 56, Vv. 3 78 575 58 56, Vv. 1 79 57) 59,60 56, Vv. 3 80 57, 61 56, Ve I 81, 82 58, 62 56, Vv. 4 83, 84 58, 63 56, Vv. 2 85 58, Report Bulletin Report V..3 86 55. vers Mien 87-89 58, Vv. 4 v. 4 90 5S. Vii3 Viens 91 58, Vv. 4 Vv. 2 92 tora. Aa | Vit) DL te Os Sas vn 2 V. 0, Dt .94 Boy Ve 4 Vi 95,901 5a. Vv. I, pt 2 97 58, Vv. § Vv. 2 98,99 59,V 2 v. I, pt 2 100 59, -¥.- i Vib kph, ) eno Bon Via Vv. 2 102 50, vie 2 Vii 2, Pt. 2. t03—5) 50.4 Vane Vit, ptsls “ro 59, Vex v.03 107 60, Vv. 2 V4 108 60, V..3 Vv. 2 109,110 60, Vv. I Bulletin Report III 60, Vv. 2 II2 60, v. I 113 60, V. 3 IT4°. 60,8 2 IIs 60, Vv. 2 116 60, v. I 117 60, Vv. 3 118 160; Vou Memoir 2 49, V. 3 3,4 53,:V.2 5,6 ° 53) Mag 7 57, V. 4 8, pt 1 59, Vv. 3 8, pt 259, Vv. 4 9 60, Vv. 4 10 60, Vv. § MUSEUM PUBLICATIONS The figures at the beginning of each entry in the following list, indicate its number as a museum bulletin. Geology. 14 Kemp, J. F. Geology of Moriah and Westport Townships, Essex Co. N. Y., with notes on the iron mines. 38p. il. 7pl. 2 maps. Sept. 1895. Free. 19 Merrill, F. J. H. Guide to the Study of the Geological Collections of the New York State Museum. 164p. 1t19pl. map. Nov. 1898. Out of rint. ep. J. F. Geology of the Lake Placid Region. 24p. 1pl.map. Sept. 1898. Free. 48 Woodworth, J. B. Pleistocene Geology of seen County and Borough of Queens. 58p. il. 8pl. map. Dec. 1got. 56 Merrill, F. J. H. Description of the State ‘Ceolobic Map of 1go1. 42p. 2 maps, tab. Nov. 1902. Free. 77 Cushing, H. P. Geology of the Vicinity of Little Falls, Herkimer Co. 98p. il. rspl.2 maps. Jan. 1905. 3o0c 83 Woodworth, J. B. Pinistoccms Sesiney of the Mooers Quadrangle. 62p. 25pl. map. June 1905. 25c. 84 Ancient Water Levels of the Champlain and Hudson Valleys 2o6p. il. ripl.18 maps. July 1905. 45¢. 95 Cushing, H. P. Geology of the Northern Adirondack Region. 188p. 15pl.3 maps. Sept. 1905. 30c 96 Ogilvie, I. Hl. Geology of fhe Paradox Lake Quadrangle. sap. il. 17pl map. Dec. 1905. 30¢. 106 Fairchild, H. L. Glacial Waters in the Erie Basin. 88p. 14pl. 9 maps. Feb. 1907. Out of print. 107 Woodworth, J. B.; Hartnagel, C. A.; Whitlock, H. P.; Hudson, G. H.; Clarke, J. M.: White, David; Berkey, & P. Geological Papers. 388p. 54pl. map. May 1907. 9goC, cloth. Contents: Woodworth, J. B. Postglacial Faults of Eastern New York. Hartnagel, C. A. Stratigraphic Relations of the Oneida Conglomerate. Upper Siluric and Lower Devonic Formations of the Skunnemunk Mountain Region. Whitlock, H. P. Minerals from Lyon Mountain, Clinton Co. Hudson, G. H. On Some Pelmatozoa from the Chazy Limestone of New York. Ciarke, 7. M. Some New Devonic Fossils. An Interesting Style of Sand-filled Vein. Eurypterus Shales of the Shawangunk Mountains in Eastern New York. White, David. A Remarkable Fossil Tree Trunk from the Middle Devonic of New York. Berkey, C. P. Structural and Stratigraphic Features of the Basal Gneisses of the Highlands. 111 Fairchild, H. L. Drumlins of New York. 6op. 28pl. 19 maps July 1907. Out ei print. 115 oes. ie are, of the Long Lake Quadrangle. 88p. 2opl. ept. I 907. 126 6 Miller W. 1 +: Saou of the Remsen Quadrangle. 54p. il. 11 pl. map. Jan. 1909. 25c. Fairchild, H. L. Later Glacial Waters in Central New York. In press. Berkey, ep; Geology of the Highlands of the Hudson. In preparation. Cushing, H..P. Geology of the Theresa Quadrangle. In preparation. Economic geology. 3 Smock, J.C. Building Stone in the State of New York. 1154p. Mar. 1888. Out of print. 7 First Report on the Iron Mines and Iron Ore Districts in the State of New York. 78p. map. June 1889. Out of print. 10 —— Building Stone in New York. 210p. map, tab. Sept. 1890. 4oc. 1r Merrill, F. J. H. Peg and Gypsum Industries of New York. 94p. r2pl. 2 maps, 11 tab. r. 1893. [50c} a: ee Boar is C ay aa of New York. 174p. 1pl.il.map. Mar. 15 Mesa °F J. H. Mineral Resources of New York. 240p. 2 maps. Sept. 1895. [soc] tS 7 Road Materials and Road Building in New York. 52p. 14pl. 2 maps. cr. 9 30 Orton, Raward. aging eo and Natural Gas in New York. 136p il. 3.maps. Nov. 1899. 15 35 Ries, Heinrich. Clays “Of New York; their Properties and Uses. 456p. 140pl. map. June rgoo. $1, cloth. NEW YORK STATE EDUCATION DEPARTMENT 44 on the Cement Industry. 332p. rorpl. 2 maps. Dec. 1901. 85¢, cloth. 61 Dickinson, H. T. Quarries of Bluestone and other Sandstones in New York. 1114p. 18pl.2 maps. Mar. 1903. 35¢c. 85 Rafter, G. W. Hydrology of New Vor State. gozp. il. 44pl. 5 maps. May 1905. §1. ° cloth. 93 Newland, D. H. Mining and Quarry Industry of New York. 78p. July 1905. Out of print. . 1oo McCourt, W. E. Fire Tests of Some New York Building Stones. 4op. 26pl... Feb, 1906. 15c- to2 Newland, D. H. Mining and Quarry Industry of New York. 2d Report. 1162p. June 1906.2 25 112 —— Mining and Quarry Industry 1906. 82p. July 1907. 15¢ 119 Newland, D. H. & Kemp, J. F. Geology of the Adirondack Magnetic Iron Ores with a Report on the Mineville-Port Henry Mine Group. 184p. 14pl. 8 maps. Apr. 1908. 35¢c. 120 —— Mining and Quarry Industry 1907. 82p. July 1908. 15¢c. 123 & Hartnagel, C. A. Iron Ores of the Clinton Formation in New York State. 76p.il.14 pl. 3 maps. Nov. 1908. 2s5¢c. The Sandstones of New York. In preparation. Mineralogy. 4 Nason, F. L. Some New York Minerals and their Localities. 22p. ipl. Aug. 1888. Free. 58 Whitlock, H. P. Guide to the Mineralogie Collections of the New York State Museum. r5op. il. 39pl. 11 models Sept. 1902. oc. 70 —— New York Mineral Localities. r1op. Oct. 1903. 200¢. .98 Contributions from the Mineralogic Laboratory. 38p. 7pl. Dec. TQOG a LGC: Paleontology. 34 Cumings, E. R. Lower Silurian System of Eastern Mont- gomery County; Prosser, C. S. Notes on the Stratigraphy of Mohawk Valley and Saratoga County, N.Y. 74p.: 14pl. “map. -May reson mage, ‘39 Clarke, J. M.; Simpson, G. B. & Loomis, F. B. Paleontoiogic Papers 1. 72p. il. r6pl. ‘Oct. 1900. |) 15c. Contents: Clarke, J. M. A Remarkable Occurrence of Orthoceras in the Gneopeat Beds of the Chenango Valley, N. Y. —— Paropsonema cryptophya; a Peculiar Echinoderm from the Intimesten® zone (Portage Beds) of Western New York. —— Dictyonine Hexactinellid Sponges from the Upper Devonic of New York. —— The Water Biscuit of Squaw Island, Canandaigua Lake, N. Y. Simpson, G. B. Preliminary Descriptions of New Genera of Paleozoic Rugose Corals. Loomis, F. B.. Siluric Fungi from Western New York. 42 Ruedemann, Rudolf. Hudson River Beds near Albany and their Taxo- nomic Equivalents. 116p. 2pl. map. Apr. rgo1. 265¢c. 45 Grabau, A. W. Geology and Paleontology of Niagara Falls and Vicinity. 286p. il. 18p!. map. Apr. 1901. 65c; cloth, goc. 49 Ruedemann, Rudolf; Clarke, J. M. & Wood, Elvira. Paleoua Papers 2.-_ 2460p. r3pl. Dee: 1991: =46¢. Contents: Ruedemann, Rudolf. Trenton Conglomerate of Rysedorph Hill. Clarke, J. M. Limestones of Central and Western New York Interbedded with Bitumi- nous Shales of the Marcellus Stage. Wood, Elvira. Marcellus Limestones of Lancaster, Erie Co., N. Y. Clarke, J. M.. New Agelacrinites. —— Value of Amnigenia as an Indicator of Fresh-water Deposits during the Devonic of — New York, Ireland and the Rhineland. 52 Clarke, J. M. Report of the State Paleontologist 1tgor. 28op. il. ropl. map, 1 tab. July 1902. 400. 63 Stratigraphy of Canandaigua and Naples Quadrangles. 78p. map. June 1904. 25¢c. 69 Catalogue of Type Specimens of Paleozoic Fossils in the New York State Museum. 848p. May 1903. $1.20, cloth. Report of the State Paleoatolonee 1902. 464p.52pl.7 maps Nov. 1903. $1, cloth. ; 80 —— Report of the State Paleontologist 1903. 396p. 29pl. 2 maps. Feb. 1905. 85c, cloth. & Luther, D. D. Watkins and Elmira Quadrangles. 32p. map. Mar. 1905. 25¢c. Geologic Map of the Tully Quadrangle. 4op.map. Apr. 1905 20Cc. 81 82 Lime and Cement Industries of New York; Eckel, E. C. Chapters MUSEUM FUBLICATIONS go Ruedemann, Rudolf. Cephalopoda of Beekmantown and Chazy For- mations of Champlain Basin. 224p. il. 38pl. May 1906. 75¢c, cloth. 92 Grabau, A.W. Guide to the Geology and Paleontology of the Schoharie Region. 314p. il. 26pl. map. Apr. 1906. 75¢, cloth. 99 Luther, D. D. Geology of the Buffalo Quadrangle. 32p. map. May 1906. 20C. ante Geology of the Penn Yan-Hammondsport Quadrangles. 28p. map. July 1906. 25c. 114 Hartnagel, C. A. Geologic Map of the Rochester and Ontario Beach Quadrangles. 36p.map. Aug. 1907. 200. 118 Clarke, J. M. & Luther, D. D. Geologic Maps and Descriptions of the Portage and Nunda Quadrangles including a map of Letchworth Park. _ Sop. i6pl. 4maps. Jan. 1908. 35¢. White, David. The Devonic Plants of New York. In preparation. Luther, D. D. Geology of the Geneva-Ovid Quadrangles. In press. Geology of the Phelps Quadrangle. In preparation. Whitnall, H.O. Geology of the Morrisville Quadrangle. Prepared. Hopkins, T. C. Geology of the Syracuse Quadrangle. In preparation. Hudson, G. H. Geology of Valcour Island. In preparation. Zoology. 1 Marshall, W. B. Preliminary List of New York Unionidae. 2zop. Mar. 1892. Free. 9 Beaks of Unionidae Inhabiting the Vicinity of Albany, N. Y. 3op. ipl. Aug. 1890. Free. 29 Miller, G. S. jr. Preliminary List of New York Mammals. 1124p. (Set, £699. Sc. . 33 Farr, M.S. Check List of New York Birds. 224p. Apr. 1900. 25¢c. 38 Miller, G. S. jr. Key to the Land Mammals of Northeastern North America. 106p. Oct. 1900. 15c. 49 Simpson, G. B. Anatomy and Physiology of Polygyra albolabris and Limax maximus and Embryology of Limax maximus. 82p. 28pl. Oct. IQOI. 25¢. 43 Kellogg, J. L. Clam and Scallop Industries of New York. 36p. 2pl. map. Apr. t1gor. Free. 51 Eckel, E. C. & Paulmier, F. C. Catalogue of Reptiles and Batrachians. of New York. 64p.il. rpl. Apr. 1902. 1§5¢c. Eckel, E.C. Serpents of Northeastern United States. Paulmier, F C. Lizards, Tortoises and Batrachians of New York. —— H. Catalogue of the Fishes of New York. 784p. Feb. 1903. I, cloth. 71 Kellogg J. L. Feeding Habits and Growth of Venus mercenaria. j3op. 4pl. Sept. 1903. Free. 88 Letson, Elizabeth J. Check List of the Mollusca of New York. 116p. May 1905. 2o0¢. 91 Paulmier, F. C. Higher Crustacea of New York City. 78p. il. June 1905. 20C. Shufeldt,R. W. Osteology of the Birds. In press. Entomology. 5 Lintner, J. A. White Grub of the May Beetle. 34p. il. Nov. 1888. Free. 6 Cut-worms. 38p. il. Nov. 1888. roc. 13 San José Scale and Some Destructive Insects of New York State. 54p. 7pl. Apr. sy 15¢. 20 Felt, E. P. Elm-leaf Beetle in New York State. 46p. il. spl. June 1898. Free. Sez 57. 23 ay 14th Report of the State Entomologist 1898. 15op. il. opl. Dec. 1898. 200. 24 Memorial of the Life and Entomologic Work of J. A. Lintner Ph.D. State Entomologist 1874-98; Index to Entomologist’s Reports 1-13. 316p. 1pl. Oct. 1899. 35¢. Supplement to 14th report of the State Entomologist. 26 Collection, Preservation and Distribution of New York Insects. 36p. il. Apr. 1899. Free. NEW YORK STATE EDUCATION DEPARTMENT 27 Shade Tree Pests in New York State. 26p. il. spl. May 1899.’ Free. 31 15th Report of the State Entomologist 1899. 128p. June rgoo. 15c 36 16th Report of the State Entomologist 1900. 118p. 16pl. Mar. IQOI. 25¢. : Catalogue of Some of the More Important Injurious and Beneficial Insects of New York State. 54p. il. Sept. 1900. Free. Scale Insects of Importance and a List of the Species in New York State. o4p.il. r5pl. June 1901. 25¢. 47 Needham, J. G. & Betten, Cornelius. Aquatic Insects in the Adiron- dacks. 234p. il. 36pl. Sept. TOOL. ARG: 37 46 53 Felt, E. P. 17th Report of the State ee 1901. 232p. il. 6pl. Aug. 1902. Out of print. Elm Leaf Beetle in New York State. 46p. il. 8pl. Aug. 1902. Out of print. This is a revision cf 20 containing the more essential facts observed since that was pre- pared. 57 59 Grapevine Root Worm. gop. 6pl. Dec. 1902. 15c. See 72. 64 18th Report of the State Entomologist 1902. r1op. 6pl. May 1903. Out of print. 68 Needham, J. G. & others. Aquatic Insects in New York. 322p. 5apl. Aug. 1903. 8oc, cloth. 72 Felt, E.P. Grapevine Root Worm. 58p. 13pl. Nov. 1903. 20¢. This is a revision of 59 containing the more essential facts observed since that was prepared. 74 June 1904. 25¢c. 76 Felt, E. P. soth Report of the State Entomologist 1903. 1150p. 4pl. I1g04. I15C. : 79 Mose ee or Culicidae of New York. 164p. il. 57pl. tab. Oct. 1904 40 : ‘ 86 Needham, ee G. & others. May Flies and Midges of New York. 352p. ral. 37 pl: June 1905. 8oc, cloth. . 97 Felt, E. P. 20th Report of the State Entomologist 1904. 246p. il. ropl. Nov. 1905. 40¢. 103 Gipsy and Brown Tail Moths. 44p. ropl. July 1906. r5¢c. 104 21st Report of the State Entomologist 1905. 3144p. t1opl. Aug. 1906. 25¢. 109 Tussock Moth and Elm Leaf Beetle. 34p. 8pl. Mar. 1907. 20¢. b & ce) 22d Report of the State Entomologist 1906. 152p. 3pl. June 1907... 25¢. 124 23d Report of the State Entomologist 1907. 542p. 44pl. il. Oct. 1908. 75e; Needham. J. G. Monograph on Stone Flies. In preparation. Botany. 2 Peck, C. H. Contributions to the Botany of the State of New York; 72p. apl. May 1887. Out of print. Boleti of the United States. o8p. Sept. 1889. Out of print. 25 —— Report of the State Botanist 1898. 76p. spl. Oct. 1899. Out og pri 28 ~ Plants of North Elba. 206p. map. June 1899. 206. 54 —— Report of the State Botanist 1901. 58p. 7pl. Nov. 1902. 4oc. 67 —— Report of the State Botanist 1902. 1196p. 5pl. May 1903. 5oc. 75 —— Report of the State Botanist 1903. 7op. 4pl. 1904. 400. 94 —— Report of the State Botanist 1904. 6op. ropl. July 1905. 4oc. 105 Report of the State Botanist 1905. 108p.12pl. Aug. 1906. 50c- 116 —— Report of the State Botanist 1906. 120p. 6pl. July 1907. 35c. 122 Report of the State Botanist 1907. 178p. spl. Aug. 1908. 4oc. Archeology. 16 Beauchamp, W. M. Aboriginal Chipped Stone Imple- ments of New York. 86p. 23pl. Oct. 1897. 25¢c. 18 Polished Stone Articles used by the New York Aborigines. 1o4p. 35pl. Nov. 1897. 25¢. & Joutel, L. H. Monograph of the Genus Saperda. 88p. r4pl. : MUSEUM PUBLICATIONS Earthenware of the New York Aborigines. 78p. 3:pl. Oct. 1898. 26c Aboriginal Occupation of New York. t1go0p. 16pl. 2maps. Mar. 1900. 30C. Wampum and sa Articles used by New York Indians. 166p. 28pl. Mar. 1g0r. 3oc. Horn and Bone Pancake of the New York Indians. 112p. 43pl. Mar. 1902. 30C. Metallic Implements of the New York Indians. o94p. 38pl. June 1902. 25¢. 50 aa 73 Metallic Ornaments of the New York Indians. 1122p. 37pl. Dec. 1903... 30C. 78 _ History of the New York Iroquois. 340p.17pl. map. Feb. 1905. 75Cc, cloth. 87 Perch Lake Mounds. 84p. t12pl. Apr. 1905. 20C¢. 89 Aboriginal Use of Wood in New York. gop. 35pl. June T905- 35¢. . 108 ‘Aboriginal Place Names of New York. 336p. May 1907. aoc. 113 Civil, Religious and aap Councils and Ceremonies of Adop- tion. 1118p. 7pl. June 1907. “t37 Parker, A. C. An Erie fadian Village and Burial Site. 102p. 38pl. Dec. 1907. 125 as verse. H. M. & Padior. A.C. Iroquois Myths and ee 196p. eeeerot, Dec. 1998. (50¢;_75c, cloth. Miscellaneous. Msr (62) Merrill, F. J. H. Directory of Natural History Museums in United States and Canada. 236p. Apr. 1903. 3oc. 66 Ellis, Mary. Index to Publications of the New York State Nat- ural History Survey and New York State Museum 1837-1902. 418p. June 1903. 75¢, cloth. Museum memoirs 1889-date. Q. t Beecher, C. E. & Clarke, J. M. Development of Some Silurian Brachi- opoda. g6p. 8pl. Oct. 1889. $1. 2 Hall, James & Clarke, J. M. Paleozoic Reticulate Sponges. 35op. il. 7opl. 1898. $2, cloth. 3 Clarke, J. M. The Oriskany Fauna of Becraft Mountain, Columbia Co., N. Y. 128p. gpl. Oct. 1900. 8oc. 4 Peck,C.H. N.Y. Edible Fungi, 1895-99. r106p.25pl. Nov. 1900. $1.25 This includes revised descriptions and illustrations of fungi reported in the 49th, sist and 52.1 reports of the State Botanist. 5 Clarke, J. M. & Ruedemann, Rudolf. Guelph Formation and Fauna of New York State. 1o96p. arpl. July 1903. $1.50, cloth. 6 Sle J. M. Naples Fauna in Western New York. 268p. 26pl. map. 2, cloth. 7 Ruedemann, Rudolf. Graptolites of New York. Pt 1 Graptolites of the Lower Beds. 350p.17pl. Feb. 1905. $1.50, cloth. 8 Felt. E. P. Insects Affecting Park and Woodland Trees. v.1 46op. il. 48pl. Feb. 1906. $2.50, cloth. v.2 548p. il. 22pl. Feb. 1907. $2, cloth. Clarke, J. M. Early Devonic of New York and Eastern North America. Pt 1. 366p. il. 7opl. 5 maps. Mar. 1908. $2.50, cloth. Pt 2, In press. to Eastman, C. R. The Devonic Fishes of the New York Formations. 236p. rspl. 1907. $1.25, cloth. tr Ruedemann, Rudolf. Graptolites of New York. Pt 2 Graptolites of the Higher Beds. 584p. il. 2 tab. 3rpl. Apr. 1908. $2.50, cloth. 12 Eaton, E. H. Birds of New York. In press. Natural history of New York. 3ov. iJ. pl. maps. Q. Albany 1842-94. DIVISION 1 zooLoGy. De Kay, James ae Zoology of New York; or, The New York Fauna; comprising detailed descriptions of all the animals hitherto observed within the State of New York with brief notices of those occasionally found near its borders, and accompanied by appropri- ate illustrations. 5v.il.pl.maps. sq.Q. Albany 1842-44. Out of print. Historical introduction to the series by Gov. W. H. Seward. 178p. - - NEW YORK STATE EDUCATION DEPARTMENT | v. 1 ptr Mammalia. 131+46p. 33pl. 1842. 300 copies with hand-colored plates. ‘ v. 2pt2 Birds. 12+380p. rq4rpl. 1844. Colored piates. v. 3 pt3 Reptiles and Amphibia. 7+ 98p. pt4 Fishes. 15+415p. 1842. pt3—4 bound together. v. 4 Plates to accompany v. 3. Reptiles and Amphibia 23pl. Fishes 79p'. 1342 300 copies with haund-colored clates v. 5 pts Mollusca. 4+271p. qopl. pt6 Crustacea. jop. r3pl. 1843-44- Hand-colored plates; pt5—6 bound together. DIVISION 2 BOTANY. Torrey, John. Flora of the State of New York; com- , prising full descriptions of all the indigenous and naturalized plants hith- erto discovered in the State, with remarks on their economical and medical properties. ev. il. pl. sq. QO. Albany 1843. Out of print. v. 1 Flora of the State of New York. 12+484p. 72pl. 1843. 300 copies with hand-colored plates. é v. 2 Flora of the State of New York. 572p. 89pl. 1843. 300 copies with hand-colored plates. DIVISION 3 MINERALOGY. Beck, Lewis C. Mineralogy of New York; com- prising detailed descriptions of the minerals hitherto found in the State of New York, and notices of their uses in the arts and agriculture. il. pl. sq. 0: Albany 1842. Out of print. v. 1 ptr Economical Mineralogy. ptz2 Descriptive Mineralogy. 24 +536p. 1842. 8 plates additional to those printed as part of the text. DIVISION 4 GEOLOGY. Mather, W. W.; Emmons, Ebenezer; Vanuxem, Lard- ner & Hall, James. Geology of New York. 4v. il. pl. sq..O: Albany 1842-43. Out of print. v. 1 ptr Mather, W. W. First Geological District. 37+653p. 46pl. 1843. v. 2 pt2 Emmons, Ebenezer. Second Geological District. 10+437p. r7pl. 1842. v. 3 pt3 Vanuxem, Lardner. Third Geological District. 306p. 1842. v. 4 pt4 Hall, James. Fourth Geological District. 22+683p. 19pl. map. 1843. DIVISION 5 AGRICULTURE. Emmons, Ebenezer. Agriculture of New York; comprising an account of the classification, composition and distribution of the soils and rocks and the natural waters of the different geological formations, together with a condensed view of the meteorology and agri- a. productions of the State. 5v.il.pl.sq.Q. Albany 1846-54. Out of print v. : Boils of the State. their Composition and Distribution. 11+371p. 21pl- 1846. v. 2 Analysis of Soils, Plants, Cereals, etc. 8+343+46p. 42pl. 1849. With hand-colored plates. ¥. °3.Fruits; ete. 84 340p.. 1851. v. 4 Plates to accompany v. 3. gspl. 1851. Hand-colored. v. 5 Insects Injurious to AsriGaltar 8+272p. sopl. 1854. With hand-colored plates. ras ease 6 PALEONTOLOGY. Hall, James. Paleontology of New York. 8v. il. pl. sq. Q. Albany 1847-94. Bound in cloth. v. t Organic Remains of the Lower Division of the New York System. 23+338p. ggpl. 1847. Out of print. v. 2 Organic Remains of Lower Middle Division of the New York System. 8+362p. rogpl. 1852. Out of print. v. 3 Organic Remains of the Lower Helderberg Group and the Oriskany Sandstone. pti, text. 12+532p. 1859. [$3.50] pt2. 143pl. 1861. [$2.50] Aa. ceil ieee eae MUSEUM PUBLICATIONS - oy. 4 Fossil Brachiopoda of the Upper Helderberg, Hamilton, Portage and Chemung Groups. 11+1+428p. 69pl. 1867. $2.50. vy. 5 ptr Lamellibranchiata 1. Monomyaria of the Upper Helderberg, Hamilton and Chemung Groups. 18+268p. 45pl. 1884. $2.50. Lamellibranchiata 2. Dimyaria of the Upper Helderberg, Ham- ilton, Portage and Chemung Groups. 62+293p. 5ipl. 1885. $2.50. pt2 Gasteropoda, Pteropoda and Cephalopoda of the Upper Helder- berg, Hamilton, Portage and Chemung Groups. 2v. 1879. v. 1, text. 15+4092p. v.2, 120pl. $2.50 for 2 v. & Simpson, George B. v. 6 Corals and Bryozoa of the Lower and Up- per Helderberg and Hamilton Groups. 24+298p. 67pl. 1887. $2.50. —— & Clarke, John M. v. 7 Trilobites and other Crustacea of the Oris- kany, Upper Helderberg, Hamilton, Portage, Chemung and Catskill Groups. 64+236p. 46pl. 1888. Cont. supplement to v. 5, ptz. Ptero- poda, Cephalopoda and Annelida. 42p. 18pl. 1888. $2.50. & Clarke, John M. v. 8 pti Introduction to the Study of the Genera of the Paleozoic Brachiopoda. 16+367p. 44pl. 1892. $2.50. & Clarke, John M. v: 8pt2 Paleozoic Brachiopoda. 16+394p. 64pl. pega. $2.50. Caiiceue of i Cabinet of Natural History of the State of New York and of the Historical and Antiquarian Collection annexed thereto. 242p. O. 1853. Handbooks 1893-date. In quantities, 1 cent for each 16 pages orless. Single copies postpaid as belo'v New York State Museum. s52p.il. Free. Outlines, history and. work of the museum with list of staff 1902. 5 Paleontology. t12p. Free. Brief outline of State Museum work in paleontology under heads: Definition: Relation to biclogy; Relation to stratigraphy; History of paleontology in New York. Guide to Excursions in the Fossiliferous Rocks of New York. r24p. 8c. Itineraries of 32 trips covering nearly the entire series of Paleozoic rocks, prepared specially for the use of teachers and students desiring to acquaint themselves more intimately with the classic rocks of this State. Entomology. 16p. Free. Economic Geology. 44p. Free. Insecticides and Fungicides. 2o0p. Free. Classification of New York Series of Geologic Formations. 32p. Free. Geologic maps. Merrill, F. J. H. Economic and Geologic Map of the State of New York; issued as part of Museum bulletin 15 and 48th Museum Report, v. 1. 59x67 cm. 1894. Scale 14 miles to 1 inch. rs¢c. Map of the State of New York Showing the Location of Quarries of Stone Used for Building and Road Metal. Mus. bul. 17. 1897. Free. Map of the State of New York Showing the Distribution of the Rocks Most Useful for Road Metal. Mus. bul. 17. 1897. Free. Geologic Map of New York. rg01. Scale 5 miles to 1 inch. Jn atlas form $3; mounted on rollers $5. Lower Hudson sheet 6oc. The lower Hudson sheet, geologically colored, comprises Rockland, Orange, Dutchess, Put- nam, Westchester, New York, Richmond, Kings, Queens and Nassau counties, and parts of Sullivan, Ulster and Suffolk counties; also northeastern New Jersey and part of western Connecticut. Map of New York Showing the Surface Configuration and Water Sheds. Igor. Scale r2 miles to 1 inch. 15¢c. Map of the State of New York Showing the Location of its Economic Deposits. 1904. Scale 12 miles to r inch. 150. Geology maps on the United States Geological Survey topographic base: scale 1 in. = 1m. Those marked with an asterisk ave alya heen pub- lished separately. *Albany county. Mus. rep’t 49, v. 2. 1898. Out of print. _ Area around Lake Placid. Mus. bul. 21. 1898. Vicinity of Frankfort Hill [parts of Herkimer and Oneida counties]. Mus. Tene St, Vs t.- 1899. Rockland county. State geol. rep’t 18. 189: i al “*Rochester and Ontario Beach quadrangles. Mus. bul. ie Amsterdam quadrangle. Mus. bul. 24, 14900. ete *Parts of Albany and Rensselaer counties. Mus. bul. 42. 190 *Niagara river. Mus. bul. 45. i1go1. 2 5c. Part of Clinton county. State geol. rep’t 19. Igor. Oyster Bay and Hempstead quadrangles on Long Island. Igol. Portions of Clinton and Essex counties. Mus. bul. 52. 1903. 20C. ; *Canandaigua-Naples quadrangles. Mus. bul. 63. 1904. *Little Falls quadrangle. Mus, bul. 77. 1905. 15¢c. *Watkins-Elmira quadrangles. Mus. bul. 81. 1905. 20c. — *Tully quadrangle. Mus. bul. 82. 1905. Free. mae *Salamanca quadrangle. Mus. bul. 80. 1905. Free. Paradox Lake quadrangle. Mus. bul. 96. 1905. ( *Buffalo quadrangle. Mus. bul. 99. 1906. Free. *Penn Yan-Hammondsport quadrangles. Mus. bul. ror. *Long Lake quadrangles. Mus. bul. 115. Free. *Nunda-Portage quadrangles. Mus. bul. 118. 20c. *Remsen quadrangle. Mus. bul. 126, 1908. Free. ; ; : , : - EDUCATION DEPARTMENT JOHN M. CLARKE STATE GEOLOGIST UNIVERSITY OF THE STATE OF NEW YORE STATE MUSEUM BULLETIN 126 REMSEN QUADRANGLE iy by WH.Lovell and GC.Bassett, * He ot ceoperation = ith Contour interval 20 fret. Drstarnn ke racears snr bavel Geology by W. J. Miller 1907 LEGEND Sedimentary Rocks Modern Valley Alluy- jum together with more or less reworked Glacial drift Lorraine Beds. Gray to black shales contain- ing thin layers of sand- stone. Utica Black Shales. Caloareous in flower portion. Dolgeville (upper Tren- ton) shales, Alternat- ing thin beds of lime- stone and shale. ————| Trenton Limestone, Including the Low- ville at the base, Coarse, crystalline, heavy beds at the sum- rolt. Metamorphic Rocks. Syenite. A rather quartzose rock, show- Ing a gnelssic strno- ture and of undoubted igneous origin, Young er than the Grenyille. Grenville Formation. Highly metamorphos- ed sedimentary rocks, showing a distinct gneissic structure and containing garnet and graphite, Syenite-Grenyille Complex. Clearly gneissoid rocks of various types, but mostly Grenville much| eut up by intrusions of syenite. Liao Precambric rocks of unknown character because buried under heavy Glacial drift Stone Quarries, PLEISTOCENE LOWER SILURIC PRECAMBRIC * i) “1 i by << - | : , " =“ > 2 | ; ~ - — i ~ r) z . : earth AG fo 286 Ome j i {, t ‘ ‘ i “ey er with, AY c) » ae} ~ si : * i | % , 7 . 1 » 4 4 he ‘ has ced t hae ee gs lg * : . . 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