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Wa 5 Wired * aes ) f a fe _ The dbjedth as cxpoael oa UN ai water-worn gravels and sands, clearly ble in certain into an upper and lower series by a thin bod’ tg 2 ial bot 0 It has not been possible in the course of the Biwi ur the area to determine whether or not the group thus det be divided into an earlier dislocated and a later snide but it is clear that many sections of these gravels, along w appears to be the boulder bed named, have been dislocated a north coast of the island. On Marthas Vineyard and Block isl lan such a division has been made out,* but the boulder clay parting, o1 the other hand, has not been found there in the position of an in iter “ mediate conformable bed. Bi iti The gravels consist of water-worn fragments of quartz deriy from veins, granite and gneiss from the ancient Piedmont terrane } n cel sda ~*~ _ “a the mainland, of silicitied fossils from the metamorphic Paleosla. $f limestones of the mainland, cherts of the same origin, and ferrugin-_ = fe ous sandstones and fragments of concretions from the underlying 2 Cretaceous or Potomac section. * 2 'McGee, W J. Three formations of the middle Atlantic slope. Am. jour. sci. Ser. 3. 1888. 35: 367-88, 448-66. It has not seemed possible at present to establish a satisfactory comparison of the deposits in this portion of Long Island with the formations recognized in New Jersey by Prof. Salisbury. * Merrill, F. J. H. N. Y. acad. sci. Annals. 1886. 38 : 341-64. * Woodworth, J. B. Unconformities on Marthas Vineyard and Block island. Geol. soc. Am. Bul. 1897. 8 : 204-11. age Paihidna except for local. apse by iron oxids. The com- pau ison with the moraines is perhaps hardly just, because the ‘moraines are locally largely composed of rearranged drift from these same beds, as in Harbor hill. The inference from the sands ; . and gravels is that they are of glacial origin, modified by the work of running water, either ice-born streams or extraglacial waters. This conclusion as to their giacial origin amounts to a certainty when the intermediate boulder clay bed is taken into the account. That the beds extend southward beyond the Harbor hill ridge or moraine can hardly be questioned; but it is difficult to distin- guish the formation in front of the moraines from the later gravels and sands washed out from the ice front. At one point in the mounded drift southwest of Roslyn an exposure by the roadside of a coarse cobble bed with yellow pebbles contains also iron stone con- eretions which have evidently not been rolled, showing that they are probably in place, though loosened by exposure to surface actions from the surrounding pebbles. Beds of this character are found at the base of the Pleistocene on Marthas Vineyard in the - Gay head section,’ where the origin of the concretions is clear. The concretions arise from the erosion of light colored clays of the underlying Cretaceous or Potomac beds and their deposition with the coarse gravels as pebbles permeable to percolating water charged with iron salts. Cementation takes place by deposition of iron oxids around all of the pebbles, involving the outer part of the clay 1 Woodworth, J. B. Geol. soc. Am. Bul. 1897. 8 : 205-6. evidence that the underlying white clays a ina oe heghng’ © ition. formity thus inferred is widespread to the east on yard and Block island and along the ‘Atlantic ¢ : the vicinity of Washington. Of direct (cel Soa said. On the shore north of Coldspring the gravelly b 1s base of the tilted Pleistocene series may be seen resting 0 Cretaceous and older clays, but there. is no observed differ a s of dip, though the absence of identifiable Eocene or Neocene beds i 8 proof of an unconformity. No clearer fact than this was gathered from the similar sections about Glen Cove and Glenwood. . Aside from this unmistakable instance of older gravels traci side of the moraine, it is uncertain to what extent the older beds r up the frontal plain. Yellowish gravels abound in the a = railroad cuts, but the yellow quartz pebbles have invariably been — washed and worn since they were stained, and similar pebbles are now working their way from the cliffs down the beach slopes into the deposits now making along the coast. It is to be inferred, how- ever, from the attitude and thickness of the Columbia north of the _ moraine that a large part of the section south of the moraine is composed of these beds. The structure of these beds is revealed in only a few pits and coastal sections. The most extensive exposures in 1900 were found ina number of sand pits on the west shore of Hempstead harbor. In these pits the beds are horizontal, and the boulder clay bed is clearly traceable. — 'Geikie, A. Textbook of geology. 3d ed. 1893. p. 146-47. aa 10q.re pT peoisduiey ‘41d 8.Sury ‘124813 SuyA[49A0 puv spues poylyeijs OY} JO OUIOS puB peq Jep[Nog SuyMoys MoIA ‘ojoyd ‘sey “HH YA OVE | rying from 3 to 10 feet in fhieleness may be seen ina posi- n to indicate that it is interstratitied with these older gravels; it _ Ses in the sand pits on St ae bay that a bed of this is de eae the a ee is a bed of boulder ae fon 2 to 3 feet thick, traceable in all the pits open in 1900 south of Bar beach. The matrix of this bed is an unctuous dark blue clay locally sandy or gravelly. Scattered through it and sometimes in close contact with each other are glaciated boulders often over 1 foot in diameter and numerous pebbles attesting the glacial origin of the deposit. Several large boulders examined in 1901 by Dr F. J. H. Merrill and the writer were recognized by the first named as having been transported in all probability from the Adirondacks. Other small boulders carrying Silurian fossils indiéated their origin in the Hud- son valley north of the Highlands. The longest journey made by these materials appears to exceed 200 miles.' The bed rests evenly and smoothly on the underlying gravelly sands without marked disturbance or erosion. This relation to the under- lying bed suggests the dropping of stones and clay from overlying floating ice more than the actual advance of an ice sheet on this part 1 Mather reported finding in the valley of Schoharie kill, poulders with ‘‘ opales- cent feldspar like that of Essex county” and referred them to parent ledges in the eastern Adirondacks. Geol. rep’t. 1843. p. 187. mack of Abs heals of gheel CR lains and sands and gravels which have accumulated a cier or its outlying stagnant masses. The bays re erosion cutting through both the Pleistocene and | Pleistocene clays and sands alike. ae A bed of till, presumably an extension of that above deal cribec oceurs on the east shore of Hempstead bay in Glen Cove sboat a feet above sealevel, in the following incompletely exposed sec ctio PLEISTOCENE SECTION IN GLEN COVE, FROM TOP Gravel and fine sand............... ss as sho Till, with small angular boulders... ... rks ee, . Gravel, clayey \'.. . fede veg sun Peo uae sate eae : Gravel; sandy. 6: 4 ee ese ee Cee 3 ae Sand, base not seen........... Jac hN se cae eanee - 20 feet distant the till passes into stratified gravel and sand. Te rapid transition of the till into stratified drift at this locality explains st the absence of the bed in many sections.. It was probably locally “a deposited. ~? A similar till bed distinetly less bouldery but equally amorphous, is exposed in the bluff at Barker point, from which, first appearing at about 20 feet above the sealevel, it sinks, on the western face of this headland, southward, being involved in the dislocations of the north coust of the island (fig. 2). *peq siq} Wot] Uaye} useq 2AvY punoise10] ul paid siapinog ey, “spues puv sjeAvis [BOv{S UooMjoq poeq Jop[nog SulAoys ‘1oqiey{ peeisdmayy ‘yYueq pues s,sury ‘ojoyd ‘sary “H & 8d oravelly sand from 6 ) feet thick, with pockets ‘lay. A gravelly till 10 thick underlies this bed, WAAR A: which again appear § PLR UZ NAVE WY, pound gravels and sand. pig. 2 southwestern face of Barker point. + the headland underlying A, cross-bedded ferruginous sands; B, the till taken place. “eee The railroad from Oyster Bay to May 4 Roslyn passes through three deep _ eat cuts in an eastwest valley in Mill he gions fy sorelesd an pete! ae Neck. In the cut nearest Oyster | lowish sandstone, with boulders; GC, Bay, whitish to pinkish sands, prob- earthy gravel ably Cretaceous, appear at the bot- tom, succeeded by about 30 feet of coarse gravels, ill stratified and 1oqivy{ peejsdmiey] ‘YUeq pues S,3uLy U! peq Jeppnog Jo Mata avaN ‘oyoyd ‘sary “H i, aS. “tena “Uh ‘ . ia “ . " \ % 33 : - ‘ , Ce a | the ere gravels eels ah ae eat evidently pertain’ the last drift. The hi Fig.7 A fold-faultin clays at southern end of Center ons show, however, island in Oyster Bay harbor _ See shat sho Columbia man- - tles over and is wrapped about masses of the pre-Pleistocene series, as previously stated on p. 622. Similar partial sections occur on Great Neck near Manhasset. — In the sand pits northwest of Port Washington, the pre-Pleisto- cene clays are also involved in folds, giving rise to a structure, the upper member of which isa gravel and sand bed of the Columbia formation, itself clearly older than the sands of the Port Washing- ton delta yet to be described (p. 646). In this instance the axis of the anticlinal structure lies north and south, and the dislocation may be of a relatively late date, even so late as the time of forma- tion of the delta named, when the ice lay deeply embayed along the north shore of Manhasset neck and when an easterly movement in the mass might be expected, since the ice at this locality was on the eastern margin of a glacial lobe at the mouth of the Hudson valley. The deposit of sands and fine gravels forming the tabular hillock whose frontage on Manhasset bay near Port Washington is known as Tom point is a unique example of the deformation and erosion of ee Gs how far this d listurbe : and how much has been done oy ‘the ¢ subsoil. shore of Manhasset bay, where the rae lalate is esse horizontal, along with the protruding masses of these older cla massive portions of the section, indicate a relatively early dis Fig.S Southward dipping flexed beds in Manhasset sands at Tom point near Port Washington, showing eroded surface same date in this portion of the island, ranging in age from at least the oldest Pleistocene to the time of the main moraines, cordial tion of * tions of t t pre- Pleis cene ba ment “a th island. would the I fore oper that the dislo- cations were | not all of the | none of them are later than the Port Washington stage. a . The upper limit of the Columbia accords roughly with the hight ee assigned to the plains described as lying north of the inner moraine, that is to say, the deposits are approximately delimited by the 200 foot contour line. Where lower, they have been eroded; where -— higher surfaces exist, later glacial drift, usually till, is found cover- ‘90R[d Ul UeeS aq 0} BIB Sdapl[Nnog euIOS puw MOZIA JO UO!JI0d deddn a} dees s{ 19}}B[ OGL “peq Jepynoq eq} WoJJ UMOp ud][PJ OAL YOIYA Slopynog Jo dnoiy “Aoqaey] pvojsdwayzy ‘yUeq pues s,3uly ‘oyoyd ‘sey “H ¢ eld he last i ice eel on » Nan their Beal i nt that these Columbia beds, exposed in fils bluffs and rraces along the north coast of the island, may once have extended much farther to the northward, but how much farther sts ‘into the area of the sound is not now definitely determinable. Their occurrence on the Connecticut mainland has not as yet been reported, and till that area is carefully studied with this problem in mind, it can hardly be satisfactorily settled. The same indefinite answer is elicited from a study of the equivalent beds on Block island and Marthas Vineyard. In other words, the precise position of the ice front and terminal moraine of this earlier ice advance is unknown, though it could not have been many miles north of the inner limit of these gravels and sands with their intercalated bed of true till. | Aside from the disturbances above noted, two classes of changes have affected these beds since their deposition: 1) the discoloration of the beds by local and secular chemical changes in the iron-bear- 1Curtis, G. C. & Woodworth, J. B. Jour. geol. Chicago, 1899. 7 : 226-36. 2Upham, Warren. Glacial history of the New England islands. Am. geol. 1899. 24:79-89, with bibliography, p. 89-92. e Bie Pecans by te gel pits on the west s sor of iron-bearing pebble has oxic ing outward and mainly are rd thro rain water, The sands and gravels above this change. . Widespread discoloration of the gravels toa doe yellow | in Roslyn in the bluffs on the east side of the town below of the moraine. This deeper and more thorough coating gravels in this locality is a natural result of the lixiviation of ferruginous rocks in the overlying moraine, the products of 1 oxidation and hydration have worked downward into the por gravels beneath. < The discoloration is therefore a change which is probably se and in progress. That it had already advanced very far before ie moraines were formed is indicated by the abundant occurrence in the moraine of yellow, stained quartz pebbles; but these pebbles in the moraine are usually not in the place in which they were original ce rs stained, for they have water-washed surfaces. The staining was accomplished while the pebbles lay in an earlier deposit, either ae Columbia or some unexposed member of the ancient coastal plain. Erosion interval. The evidence of late dislocation on a small scale commensurate with the pushing and dragging action of a— great ice sheet, the spreading of till and boulders over the surface : =. of the Columbia, and the amassment of heaps of drift evidentlyin part derived from the surface of the deposit, afford indubitable evi- dence of the degradation of the formation to some extent by ice gs action subsequent to the completion of the series of deposits. But JOqivpy{ pvosduieyy ‘YuRq pus s,Supy ‘seqsem pueg ‘ojoqd ‘sary “H a > . ao es etd So) Y MEL pnione into Meant 3 that in whose lower extension Mill | ane Gen it must be aaluetisd subglacial drainage may have followed the course of this valley for a part or a whole of course. The objections to accepting the valley, however, as the work of this subglacial stream, aside from those above stated, are om m3) the graded character of its bed, sloping northward toward the oe sea as if made by a normal stream like that now flowing in it, ak though the existing stream evidently flows in a valley which it - found encumbered by more or less glacial drift; 2) the tributary vales evidently cut by running water as in normal open air streams ; 3) the course of the stream at Glen Cove, east and west, in a direc- tion contrary to ice movement in this locality. The digitation is even more pronounced in the case of the Mill Neck creek valley just south of the ponds. The upper part of the valley above the 100 foot contour is also walled in by glacial deposits later than the Columbia in which it is cut. Like considerations hold in regard to the deep valleys which extend from Oyster Bay village toward East Norwich. The Mill Neck creek depression continues below sealevel, and, branching south of Oak neck, separates that island — an island except for the barrier beach tying it to the land on the west — from Mill Neck. It is evident that there has been developed a marked dissection of the Columbia, and that this dissection on north and south as well as on east and west lines is increasingly severe toward the northern coast, as in the normal degradation of an area of incoherent materials marginal to a depression such as that of of the pateebaioge Get r deposition — probably small ¢ extending above sealevel —and so deposition by tides and currents. A these embayments ecbenguent to ‘the port harbors. They are also found on Marthas von in pond and Menemsha pond, and on Block island in Great p m1 As to the period of this valley-making, excepting the modi and enlargement by ice action, it is clearly older than th or ‘inner moraine at Roslyn, a deposit believed to be equiv the Cape Cod moraine. Whether the stream erosion preced followed those fragments of an older moraine which on this & 3€ mark the western extension of the outer or Nantucket moraine appears to be locally undeterminable, because the two sets of p nomena are not found in association. If a comparison with Mart. Vineyard and Block island holds good, the erosion of the valle should be here as there anterior to both moraines. In all of these — New England islands, the valleys do not occur as such on the one 4 of the moraines, because that area has been buried beneath the out wasli plains of the first or outer moraine on the eastern islands onde of both the first and second, or inner and outer moraine on oe Island. | The time involved in the excavation of these valleys is indetermi- nate. They are largely excavated in gravels and sands of a porous structure. Much of the existing rainfall passes through the lin in ou area ee sibcady bees * 7 ont inf the topography. Both of these deposits ely composed of materials which have been water-worn, eature retlecting the nature of the terrane from which the rials were eroded and on which they were deposited. The ice 2et on leaving the bed rocks of the mainland and the north shore and pais aalarane debris frets these older water-worn deposits ; hence the water-worn pebbles which abound in the moraine even _ when the materials are truly ice-laid without stratification. True te. clay occurs in small patches, but much of the till is sandy, and even in its coarser phases often exhibits traces of water action closely followed by a shoving of the deposits into contorted drift. The outer deposits consist of a few low knobs rising like kames from the surrounding gravels. They bear a few boulders on their surface and frequently in road euts reveal a thin patch of till. West of Searington rolling surfaces of till composed of a gravelly boulder clay give the deposit, along with its steep southerly front, something of the aspect of the main moraine as it exists southwest of Lake Surprise. These knobs and their rare attendant basins have a much less strong development than those heavier accumulations which lie in the form of a strong ridge immediately north of them. The deposits do not afford in themselves precise indexes of the posi- tion of the ice front at the time they were made. They appear to be submarginal deposits laid down when the ice front lay somewhat to the south of them, and are best compared with the kame moraine in the eastern part of Nantucket. The inner or main moraine exhibits likewise the two phases of 5 ee on water-worn gravels et tee a ne an mace of the knobs is furthers —_ ed 1 Westbury sae Their massiveness ane accordance it ey with the inner ridge are good evidence that they were | form the same phase of ice action which was concerned in the cons tion of the main ridge of which they are but spurs. o - The thick till phase of the moraine proper shades off. ceptibly into the thin till phase of the upper surface of ches ravel plains on the north. This latter drift appears to be, over me st | t of the area, ordinary ground moraine like that on the na Ps north of the moraines. Only here and there and viartisuiaidl on t extreme eastern border of the Oyster Bay quadrangle do consider able patches of till with morainal topography lie north of the nigel wall, but none of these have the aspect of a frontal deposit. They a = are, rather, thickened deposits of the ground moraine, and thelr "ae principal relief is molded on the ridges and valleys of the older — a | : % ; drift which they mantle. They have therefore on the map been distinguished from the deposits which by their linear arrangement — and massiness more clearly pertain to deposition at or immediately beneath the ice front. The stratified gravels in the moraine appear to belong to two dis- tinet categories as regards the mode of their origin: 1) ontwashed gravels laid down at the ice front and subsequently pushed up into —* ridges; 2) high cones or fans deposited along the ice front by out- pouring streams either from fountains such as Russell has described aor Phe. 4 Upham, Warren. Glacial history of the New England islands. Am. geol, 1899. 24: 79-89. §’Chamberlin, T. C. U.S. geol. sur. 3d an. rep’t. 1883. map, pl. 33. aged a wr lf the land serratlig waciciius ol tie tt inlar ‘tr made in the fall of 1900 by J.B, Wax dm: extension of the inner moraine to tlie so hwest on to the eastern limits of the Oyster Bay quad : This interpretation of the westward oxtousioo'el sist is quite in line with the observed tendency of the ice fi southern coast from the easternmost point in Miideahit s to Hudson river. On the east the moraines of Nentackée n a ; Cod are at the outer margin of these two lobes more than § > miles apart. In the region of Vineyard sound they are from 5 to 10 miles apart; they are quite 10 miles apart in the meridian of E lo k island; when they reappear on Long Island, they approach each other. West of Roslyn, the second moraine crosses the first. é aa this it is concluded that the inner moraine is not so much ar sional moraine as a frontal moraine built after a retreat frou re position of the first moraine, followed by an advance to the oon ee of the second moraine, accompanied in the Hudson valley by a. ay “2 greater outrun of the ice sheet than in the first advance. This overlapping of moraines is a well attested phenomenon in the ream x 3 south of the great lakes. "Oh The ice front which rested against the north coast of Long Talal in the vicinity of Port Washington can not well be the same as that _ whose moraine caps the cliffs east of Port Jefferson. In the first place, at Port Washington the morainal accumulations are very slight indeed and do not rise in mounds; in the second place, the ice sheet halted there for a brief time only, as is witnessed by the small amount of outwash in the sand plain at that locality. This oe a . -~ 7 —,. e (ii a PLEISTOCENE GEOLOGY OF NASSAU CO. AND BOROUGH OF QUEENS 643 halt is rather to be compared with those nearly stagnant ice fronts which are marked over southeastern Massachusetts and in the Nar- ragansett bay region by similar sand plains formed in the retreat of the ice from the long maintained frontage on and against the Cape Cod moraine, a stage everywhere on these islands marked by well developed outwash plains. Glacial streams. The course of glacial streams escaping from the ice front and extending over the frontal plain on the south side of the island is plainly indicated by the creases extending from the moraines near the head of the north shore harbors and from other passes in the main moraine. The principal of these streams seem to have followed the course of the harbors, if we may judge from’ the cross-section of the erosion channel or interruption of the moraine where they crossed it.. The most instructive of these chan- nels across the moraine is at Roslyn; there is another at Manhasset, and still another less marked at the southern end of Greatneck bay. In each of these cases the larger valleys quite up to the pass in the moraine appear to have been occupied by ice at the time the ice sheet began to melt away. The thalweg north of the pass or divide rises steeply, usually from the bay side, invariably much steeper than the gradient of those valleys which, elsewhere on the surface of the plains north of the moraine, have been interpreted as older than the last ice advance. The pass in the moraine north of Creedmoor at the southern end of Little Neck bay is about 150 feet above sealevel; that of Manhasset bay is about 170 feet. The Ros- lyn channel is at about 130 feet. There is thus no accordance of level in these outlets. Other passes across the main or inner moraine occur west of Ros- lyn at about 230 feet, and east of Harbor hill at about 90 feet. Southeast of Brookville there is a pass at about 230 feet, and south of East Norwich another at about 210 feet. All of these appear to be more or less in line with certain valleys north of the moraine, and all of them lead out south of the moraine into creases which descend to the sea. The broad depression passing by Locust Grove toward East Nor- wich is not wholly erosional in origin. Just north of the road at Locust Grove the bottom descends into a large elliptic pit suggesting thesea, ap Ara, The frontal wlio near + Oneodiadee crease, and many creases which are distinct on margin of the outwash plain become faint Here actic as surface features nearer the moraine. This fading would be caused by the wandering of streams over ithe a f spreading gravel and sand, with the aggradation or building a the plain by the streams near the ice front so long as they BY overloaded with debris. | The creases on the eastern part of the Hempstead quadrangl deflected southwestward into the Jamaica bay depression. Ea that region, the streams flow generally southward, the numer ous creases inarked by the 100 foot contour line, for instance, gat ne ‘i southward into six or seven drainage channels through which sm: streams now drain the water from the plain. 7) RS Outwash plain. The outwash plain is evidently more complex eos in its origin that its mere surface would indicate. The disap- pearance of the older Pleistocene gravels beneath the moraine on ma, the north at about 200 feet above the sea has already been noted. __ Just as the level of these deposits falls off on the north side of the See moraine to the westward, so does the hight of the outwash plain, and, for that matter, that of the main moraine itself. There is good reason for holding therefore that the so-called Columbia deposits extend south of the moraine and presumably underlie the outwash plain, if they do not actually form here and there surface exposures. ely element fas ae upper oe of the section of Ss s the brick clay found at ae Williston. While clays ve sea, to Be subsequently pi erlaie by the outward growth 3 thickening plain, such clays would hardly be formed with a o nearly that of the completed gravel plain ; and it is prob- able ‘that these are either an older degraded deposit or owe their Seiten to the deformation and uplift of the basement on which the deposits and topography of the last extraglacial streams have been imposed. The section, which is exposed in a somewhat depressed, troughlike area, is as follows: — SECTION OF CLAYS AT EAST WILLISTON Feet 0 A lee ee iy dx ane gh oa IY ee Mas Sand, gravelly, with quant and granitic pebbles, locally red- RMN rE SS 5.55.0 tae tanta lem we lad step as net esi we 8 Clays, sandy, with quartz pebbles...... We Rie oer ee Clay, sandy in yellow band......... Bi sv niaste ASAT athe Clay, blue, finely laminate, rarely with ies pebbles, PmpoOped ss... .. Sree ten PED ect ge eee See Oe on es The section is apparently conformable throughout. Crosby, if I understand him rightly, would refer these clays to the Tertiary. The manner in which the water percolating through the sand plain north of and above the 60 foot contour in the Hempstead tation Biahd la eat rlike ridge ville ; a oe ce r, mu than its southeastern face, is not conelus | : Bs the northern margin of a frontal deposit up against the base of the ice front. If this depos » such an origin, its northern slope would fix the front of t Ac the time of the making of the outer line of morainal depocitag half a mile in front of the submarginal moraine, and this gravel would somewhat antedate the part of the creased plain lying tot t west. | rT re —: The plain everywhere on the south sinks beneath the surface of the marsh without trace of a shore line action. So far as its present f surface is concerned, it appears to have arisen by the outwash ‘ streams in the manner of those extensive sheets of gravel, sand, and glacier mud which confront the Malaspina and other existing ee ; ciers in high latitudes at the present day. BP With the completion of the inner moraine and the sheeting over hic ; of the southern outer slope with gravels and sands creased by out- running streams, the principal work of the ice sheet on this portion of the island ceased, and we next find indications of its front farther — north along the blufflike descent to the present Long Island sound. This front is best marked at Port Washington and on the area to the > westward shown on the Harlem and Brooklyn quadrangles. Port Washington stage. The first definite trace of a halt in the ice front after the retreat from the main moraine is found on the northern and western extremity of Manhasset neck near Port , : [@A9[B9S JUISOId GAOGE 499J OS JNOge je VI[OP OY} JO GOBJINS [PAG] OY} PUB ‘Speq }oeS-dO} UlYq} EY ‘YINOS ey} P41BMO} Bajddip speq 3es-910J Suymoys “oaoqe YNiq Wood) MAA “UOUSUIYSeA WOg ‘3)d pues s,ABIIN| puke pssy ul B)[ep [BTOR[s Jo uoT}0eg ‘ ‘ojoyd ‘sary "H a and ith: a hte margin. These vard fr m the east and the north and have their sum- od by the 80 foot contour line. | The plain of sand is boulders, and its structure, as shown in numerous deep consists of beds dipping everywhere southward toward re at angles of about 20°. All about the iceward edge of % | plain are boulder-strewn fields, which on the north and : west have a decidedly moraini¢c topography below the 100 foot con- tour line. — _ From near Plum point around the coast of the sound to ce Mott point this topography is very distinct, forming a rough slope ee am to the ‘sea rather than a ridge; but the morainal deposits, as shown “ab: Barker point, are a mere veneer over older glacial beds. The topography thus defined marks the overlap of the ice sheet at this stage on Manhasset neck, and the sand plain is a delta formed in a body of water whose surface was approximately at the level of the summit line of the lobate margin of the deposit. It follows from this conclusion that, if other sand plains at this level oceur to the east and west on the north side of the moraine within approximately the same distance of retreat from the main moraine, the probable position of the ice front at this later stage may be traced by drawing a line along the northeru margin of these deltas. Another such deposit less clearly developed occurs at Great Neck village at approximately the same hight; and, as the line between the inner margin of the sand plain and the ice edge on the western part of Manhasset neck turns in this direction, it appears legitimate to associate the two deposits in the manner indicated. The line thus drawn suffices to show that the front of the ice sheet was at . alice rete purpose eof eoinpaiieon and in. detinite conclusion the problems arising on the area with, a reconnaissance was made of the. og gion on tl 1 questions which have thus far arisen are the distin netic inner and the outer moraine, the nature of the water | 20 the Port Washington delta was deposited, and incidental he son for the diversion of glacial drainage on the outwash plai | Jamaica bay. ay, a It has been shown how the “inner ” moraine becom principal and outer moraine west of Roslyn. From this: particularly near Hollis, to the western limit of the island t ment of the front of the moraine at its merging into the sam is strikingly uniform in direction. From 2 to 3 miles eas west of Jamaica this line certainly is suggestive of an ancient | line, now at about 80 feet above the sealevel. % A number of newly cut streets expose the glacial deposi this line, particularly on the crest and frontal slope of the mor in the vicinity of Jamaica. The moraine near the front is al of till with medium-sized boulders, often passing into an ill strati- fied, contorted drift, with lenses of till and gravel, the ‘opagaea of the whole being of the knob and basin type. The frontal slope of the moraine inclines from 15° to 20°, an ay < ce t ' On the colored geological map accompanying this report, the deposit at Great — Neck village is not discriminated from the older Manhasset sands for the reason that no section of the deposit was obtainable. e PLATE 1 BULLETIN 4a UNIVERSITY OF THE STATE OF NEW YORK PREDERICK J.H MERHILL, DIRECTOR & STATE GEOLOGIST STATE MUSEUM : dyhtit: aN : ee OF THE A a OYSTER BAY AND HEMPSTEAD QUADRANGLES E jelancey Pr. Be LONG ISLAND Ls i ZA : S ae E : LEGEND RECENT Matinicock Pt AND NOW FORMING ; Marine alluvium; | } beaches of éravel and sand | | i SLXECUTION ROCKS LM rok See Es 3 ‘> Bolian deposits; i> 4 ‘i dunes and blown sands PLEISTOCENE Glacial sand-plains, Port Washington stage; d gravel (Harlem Prospect Pt north of the inner moraine WISCONSIN EPOCH OR LAST GLACIAL \e areas boulders, mnarlané outer moraine The outwash plain Sravel and sand of anhiasset boulder bed) Slacial depositin Manhasset sands PRE-PLEISTOCENE OLDER PLEISTOCENE Far Rockaway gravels; w gravels Gretaceous clays and sands turbed positions & Graveland Sand pits 5 Clay pits et inoline pits Boat Garden ees /| pP flerfipnte dd. Pond. M AL (Brooklyn! Topography by U.S. Geological Survey in espperation wich the = 7 — tate Engineer and Surveyor a 2 a leistocene Ge 2 « - SS) » _—$ Milos by J.B ee ad Contour interval 20 fear, 7 Danan ts mean rea level, | YABB. LYOW, STATE PRINTER, a n ent back by wave | el - margin <3 the frontal plain, then bend downward into kettle-hole i in the deposit, a Cepression marking the site of a mass: ‘of ice. The attitude of the beds suggests frontal shoving on ie part of the ice sheet as well as irregular deposition; but the Peasant feature at this locality is the apparent absence of any- thing like a cut bench or cliff in the bulging front of the deposit. The structure of the sand plain is exposed in occasional pits. The beds are prevailingly cross-bedded, showing frequent reversals in direction of the transportation of the sediments. Such cross- bedded Jayers occur in glacial gravels where there is no reason for supposing the sea to have acted on them. On the east, on the Oyster Bay sheet, the inner margin of this frontal plain rises above the 100 foot contour level; in this region it sinks gradually below it, till north of the Jamaica bay depression, where the plain has a width not exceeding 14 miles above sealevel, its hight next the moraine is only 60 feet ; westward it rises shghtly again. Fora portion of its length, therefore, this line accords in elevation with the 80 foot level of the water body in which the Port Washington delta was built. If throughout the line accorded with the Port Washington level, it would favor the existence at that stage of a body of water in front of as well as in the rear of Washington stage of ice ee The semicircular area of Hey and « Si bay outlines a remarkable depression in th “ moraine immediately back of it is quite as well some distance east and west of it, nor is the crest perceptibly lower at this point, where there ap] ye rs of development of the plain. The moraine she ws the signs of having been depressed at this point, and was orn ably later than the depression referred to. Ae That this depression in the plain is a feature dat ng fr g'acial times and an original feature in the growth of be eo also shown by the behavior of the creases or drainag which lead into the bay: these creases converge on all si the depression, showing that the slopes of the plain » now toward this relatively unfilled area. It follows there the plain has not necessarily been deformed sinee glacial ti - that the rising and falling of the inner line of contact of the with the moraine is an original constructional characteristic of deposits. If this reasoning be correct, then the local coincidence ict level of the inner margin of the plain with the level of the Port | Washington delta is not due to the control of a water level common to both areas. ‘iyie Moreover there is reason to believe that the frontal plain was iainly developed when the ice lay along the inner moraine pre- vious to the Port Washington stage, and, as will shortly be stated, that the Port Washington delta was deposited later in a temporary lake confined between the moraine and the retreating ice front. Binnd; cece 0 ee cone oF the Far ierends ridge, was ; but the following well section, reported by Dr. F. t? H. Perera years ago, would seem to indicate that the Far ay gravel extends in that direction. The normal sediments ep plain would be, at least at surface, at this distance ; i WELL SECTION ON BARNUM’S ISLAND? — "Feet | Sand and grave, stratified........ it? PI ed cea eng oh nl ia Se Geetmand clayey sand with lisnite.....0.220.....0..000.0, 56 Gravel and fine sand with clayey sand.................... 44 Blue clay, clayey sand and silt, with lignite and pyrites...... 168 Crosby agrees in referring the upper 70 feet to the yellow gravel. The elevation of the ridge is quite uniformly a little more than 20 feet above the sealevel ; its direction is parallel with the moraine on the north of it. This association of a depression which appears _to have been in the process of filling by streams pouring from the ice front, with a bar of gravels older than the outwash plain, as their composition and form show, suggests the deformation of the Columbia or some underlying coastal plain formation at some time anterior to the completion of the moraine and its frontal plain. Such deformation might well arise as the effect of the imposition of the weight of the ice sheet on the yielding sediments previously deposited. In this view, the Far Rockaway ridge is an outlying, upraised fold, or “ parma,” ” and the bay a correlated depressed area, 1Merrill, F. J. H. Geology of Long Island. N. Y. acad. sci. Annals. 1886. 8 : 350. 2 Suess, Edouard. La face de laterre. Paris. 1897. 1: 820. of west, forming ¢ a preps. fs: : ‘ in New Jersey, glacial striae in this part to the east of south. A number of ledges City meet this requirement. One of the larg rock occupies a vacant lot adjoining the Queens ¢ , w on the west. The ledge is heavily glaciated, forming a C roche moutonnée. The striae range in direction from 2 ee west (magnetic). A few striae run from n 15 w, and on e set scratches lies in a northwest direction. The strike of the f oliati of the gneiss is n 25 e magnetic. Other outcrops occur to the east with striae running from the north northwest. piles: . shallow oval depressions extends in a northwest and southe tion across one outcrop, the whole bearing evidence of water a presumably that of a subglacial stream. : The southeastward movement of the ice on this side of the I ‘son valley is further attested by the drift. The moraine fi srooklyn as far east as Oyster Bay contains trap boulders, the nearest known site of which rock is in the Palisade trap ridge on . the west bank of the Hudson river. ow Stratitied red sands, also undoubtedly derived from the area of * Triassic red sandstones now found only on the west bank of the Hud- is son, occur in a section by the roadside from Corona to Astoria, being there overlain by 8 or 9 feet of gray till with trap boulders.’ ' Boulders of trap and red sandstone were seen by Sir Charles Lyell in an exca- — vation made ina boulder bed at the Brooklyn navy yard, See Lyell, Charles. Travels in North America. N. Y. 1845, 1: 189-90. PLEISTOCENE GEOLOGY OF NASSAU CO. AND BOROUGH OF QUEENS 653 This fanning of the ice sheet to the eastward on the east side of thé lower Hudson and to the westward on the west side is consistent with the form of the moraine across the mouth of the river. The axis of the lobe thus indicated has been fixed by Salisbury on the west side of the Palisade trap ridge.! From what has been stated, it would appear that the western end of Long Island is occupied by a moraine and a contemporaneous outwash plain built along the margin of the ice sheet, when it had, in this region adjacent to the mouth of the Hudson, pushed a lobate mass somewhat farther south than the limit attained by an earlier stand of the ice front, marked eastward by the outer moraine from near Roslyn to Nantucket ; that the frontal plain in this district rises to slightly different levels against the front of the moraine, a feature which is constructional and not due to post-glacial warping ; and that the front of the moraine as a whole presents no decisive evidence of having been subjected to marine action above the present level of the sea. With this statement of the observations bearing on the marine limit at the time of the last ice invasion, it is necessary to return to the later ice phenomena exhibited in connection with the Port Washington stage of the’ retreat. Port Washington glacial lake It has already been pointed out that the last evidence of the pres- ence of the ice sheet on the area covered by the Oyster bay quad- rangle is found in a well defined delta and attendant ice-laid deposits occupying the semicircular tip of Mannasset neck. The phenomena indicating a halt of the ice front against this headland for a brief time subsequent to the retreat from the inner moraine at Roslyn are very clear. The conclusion having been reached that the area has not been submerged to the depth of 80 feet since the beginning of the deposition of moraines in this part of the island, it seems neces- sary to further examine the region to determine the possibility of this delta having been built in a temporary glacial lake. To the north and west of Port Washington occur a number of gravel and sand pits opened in a characteristic glacial delta, whose ‘Salisbury, R. D. N. J. geol. sur. An. rep’t state geol. for 1898. 1894. p. 161. The tee uke pl a or d bay, trending northward fromi>Pbrit Wi ward about one mile beyond the village. accordant with the outline of the outer c a a of distance varying from half a mile to a lee te t he lo stratified sands pass into till, and the level sur ‘ ace ¢ gives place to a hummocky topography, sloping generally t the open waters of the sound, plainly indicating the de Me ee ri were laid down in the presence of the ice or beneath it wl waters pouring from the ice constructed the delta, — We a 1 the picture of a small semicircular embayment of the ic f From an inspection of the ground, it appears that the e t th ice lapped over on the existing land for a distance of three fo urths of a mile to nearly a mile from Barker point, around by Sands Lig point, and for a slightly greater breadth on the eastern aide tO least as far as Mott point. Beyond this locality it is quite impo eibl eo hale to discriminate the deposits of the ice made at this stage frou th earlier deposits laid down when the ice front was closely pres against the moraine on the south. , aa The structure of the delta as exposed in the summer of 1900 is typically deltiform, with beds of sand steeply inclined toward the — frontal lobes, each bed having been deposited in its present inelina- tion on the growing edge of the delta, as the streams coursing over the embankment, already built up to water level by this process, came to the outer margin and let their load of sand come to rest by sliding down the frontal slope to the angle of repose for that material in water. (See pl. 7 and 8) ae vf ‘ 3A is Pilate S H. Ries. photo. Section of glacial deita in eastern sand pit, Port Washington, showing fore-set and overlying top-set heds. View looking north w ae was ce off from is sound along the sorthe and, and that the sound was as yet filled with glacial 3 of Port peseaneton mies: there isa deep channel u aot Be an: northeastward across the eyelia and till io: ie Seavey: of Mott point. ee bottom of this trough, ae ve the ent ae The trough has the form of one of etd _ those creases eroded or kept open by water flowing out of the ice 3 2et or from one glacial lake to another along the ice front. At | ‘the time it may have connected the waters confined in Hempstead bay with the water held by the ice sheet in the Manhasset bay depression. The crease at the southern end of Hempstead bay, at ‘Roslyn, shows clearly that a stream once discharged there across the moraine on the plain, with its bed over 120 feet above the present sealevel. Hempstead harbor is bounded on the east quite up to the sound by land rising above 100 feet, so that, when the ice front retreated from the morainal wall at Roslyn, drainage would continue to escape through the Roslyn channel till the Mott point channel was opened by the retreat of the ice north of that point. At this stage any open water in Hempstead harbor would have escaped into the Port Washington body and its level fallen off to about 80 feet. This arrangement of cols and drainage channels, considered in relation to the retreat of the ice front, proved by the Port Washington stage, in Manhasset bay after the ioe front h ad ta ire Washington, for the water level had then ‘fall on nessed by the delta at that locality. eo waa Bi ‘ West of Manhasset bay, most of the sage | fails to attain the 100 foot level. The moraine itse tinuous barrier rising above the 80 foot contour line a the vicinity of Maple Grove is reached. Between this 1 Prospect park in Brooklyn, there are eight or nine low, Trou passes across the crest of the moraine, which might have serve the overflow of water held in on the north between the mo ‘ the retreating ice front as late as the Port Washington st the ice, on account of its greater activity near the axis of son lobe, maintained its position close to the moraine in the v: vi on] of Brooklyn, at least depassing the 80 foot contour line on the be ie of the moraine so as effectually to prevent discharge by a 1a F level into New York bay north of the Narrows. Bae These troughs across the moraine are singularly uniform in leve In all those enumerated their bottoms lie according to the govern ment survey between the 100 foot and the 80 foot contour Tinga,” if x . Some of them are clearly inosculating kettle-holes, marking the site 3 & of melting masses of the ice. From some of them, drainage creases _ aa can be traced out over the frontal plain. They are best developed in line with the bays and depressions on the north side of the tnoraine, and hence were probably the paths of subglacial streams, as in the case of the passes on the Oyster Bay quadrangle. They are however not unique in this portion of the moraine. There are PLEISTOCENE GEOLOGY OF NASSAU CO. AND BOROUGH OF QUEENS 657 other similar passes at higher levels. Their coincidence of level is apparently accidental ; but their repetition not only determined the level to which delta construction should reach in the temporary lake behind the moraine at this stage, but the fact also explains the failure to depart from that approximate level while the ice main- tained its position. With the possibility of the water spilling over through several or all of these channels, the drainage, if the time were short, would hardly concentrate on any one of them. That the time was short, is shown by the small delta built at this level. Where the outpouring stream from the ice was strongest, the delta pushed out about a mile. The deep drainage furrow dissecting the delta on a north and south line indicates a sudden falling off in the water level. This undoubtedly points to a change in the position or in the solidity of the ice barrier on the west, such as to permit the confined waters to escape into New York bay at a lower level than the passes in the moraine. The fact of such a change of level is indicated in a small delta at about 40 feet in the vicinity of College Point. College Point delta A poorly developed delta fringes the southern slope of the bar of glacial drift which connects College Point with the village of White- stone. The northern slope and much of the crest of this ridge are morainal, though sands are exposed here and there beneath this ice- laid coating. Ata point about due south of the bottom of Powell cove, a section open in June 1900 showed the fore set and top set beds of a typical delta structure extending southward. The struc- ture as in fig. 9 indicates a period of building at about 35 feet above the present sealevel, followed by a rise of the water level of about 5 feet, the whole indicating clearly a water body north of the main moraine at about 40 feet above the present sealevel. The ice front had now evidently retreated along a part of the line somewhat north of its position at the Port Washington stage. That this retreat was not without slight advances, is probably indi- cated by the evidence of rising water level in the College Point delta; but the opening of crevasses in the ice margin and their sub- Brooklyn into Wallabout aie the hi the 20 foot and 40 foot contours. From 7 winding passage below the 40 foot level | W charge into or connection with Gowanus | moraine at the Narrows. s : & i “a ieee F Fig.9 Cross-section of the structures observed in the Col- stated chan simi lé r 2 bebeepelnya ste: fore-set beds; b, top set beds; c, mations north of moraine indicate v spread waters at about this level. When these have been - rt investigated it may be necessary to admit a submergence to. extent. What is stated here must be taken with this resers in mind. ee alae ' See, on the formation of temporary lakes at the present time, Edouard Suess, ey La face de la terre. Paris, 1900. 2:590-97, and the authors there cited; alsoDe Lapparent, Traité de géologie. 4meed. Paris, 1900. p. 302-3, on the sudden _ we drainage of glacial lakes. For American glacial lakes of the class here described, ; we H. B. Ktimmell, Lake Passaic, an extinct glacial lake, in N. J. geol. sur. an. rep’t for 1893. 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Min of New Y detailed deseriptions of the minerals hitherto wanes we York and notices of their uses in ok gibsite dh communes ‘i ple @ 1842. Out of print. DIVISION 4 GEOLOGY. Mather, W: W Ebenezer ; ; Vanuxem, L & Hall, James. Geology of ‘New York. ear ek amg pl. sq. Q. Albany Out of print. DIVISION 5 AGRICULTURE. Emmons, Ebenezer. Aertpultiry of New York; co prising an account of the classification, composition and of the soils and rocks aud the natural waters of the different is gros ations together with a condensed view of the eerie | hee sgricoltara duc tions of the state. 5v. il. pl.sq.Q. Albany “Te DIVISION 6 PALEONTOLOGY. Hall, James. i misled AO. of ee ae pl. sq. Q. Albany 1847-94. Bound in cloth. Museum handbooks. 7%4x121%4 cm. Albany 1893-date. Price in quantities, 1 cent for each 16 pages or less. Single copies pe as below. Hs5 New York state museum, 14p.il. 3. Outlines history and work of the museum; with list of staff and publications, 1893. H13 Paleontology. 8p. 220. Brief outline of state museum work in paleontology under heads: Definition; a to biology; Relation to stratigraphy; History of paleontology in New or HI5 Guide to excursions in the fossiliferous rocks of NewYork, r20p. &8. Itineraries of 32 trips covering nearly the entire series of paleozoic rocks, pre- pared specially for the use of teachers and students desiring to acquaint tiem selves more intimately with the classic rocks of this state. H16 Entomology. 8p. Out of print. H17 Geology. Jn preparation. Maps. Mermll, F: J. H. Economic and geologic map of the state of New York. 59x67 cm. 1894. 25¢. Scale 14 miles to Linch. New edition in preparation. Geologic map of New York. 1901. $3. 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