we 2 4 i+ q ‘ Pane ‘ i ua piel nae Pitted ne dee gat pe bel Ae pied Ltt ee tite * aa A dy eae PG She 0 Beas dts cde etal vari esd or Hike tae? te aber eid Rt Lie ear bce cee fae i by ne Taare + BIT wo 56 capte pace hee eat ae OF: Sedei od eas beat dt ny tune eet oy her ted Ped © bbe ceaatian peat we age ee werar ie yt y ea pa ad PPT re rate) ue MGay Waymrarecs egy Pk A Cry obese Or ere o fas eile ete ; ton mabe oe “ a vie wpeaed ke) poe abe ae AS, ‘ ‘i 7 ‘ the ner Fy flee ag io = X “as 2 | i hy : TOT ML AL Lid pee y oD nn AMINE = iat tah eh heh ee . ys 5 suite ae PDD A AAIAT TN | : ‘ a e Sug * : 3 : mete fe a ig) eo gyal yest y VoUe ; ‘ arava a ty os tet A 4 ‘e we wi raf ees ees 4 tee g as atahn id 4,_¢ wty oN aad | ern \% 5 a = gi ALN ee UN iwaser~ ype Witty oe ae ee ; Wisi Worn etree uta tate ull epee ‘ Wyner j TS OF Dt vee “tT ) : Tstwy : = De NS eT ANITA AAA BATH 6 ¥ US a ~ wav | AA we! byte eye Smee cake aweztas . heeeed |) Sa ROS 8 ahd Ve weNere MNT vee vy : SoS ‘ ; : : Br, i & 4 Se vy ; — = } g Y yey ww 2 it & ce= ~g9VT 4s eee Ripe Dh ikea da hl fei dea Liphh i eal woth nal aa F mote | 7 Lz VUEe | hal dh | RA ey Re es £59 Se OR, : te ee BE , we Ne padded ed SO : 3 ‘ 5 4 % wed Sy bee fut = ¢ ” COLT Oe - APs, | ww ee & 5 eS es yy Ye S eel ow Ap A» siggy eg ew pet 4 eA bbl | gOS eeice e a thy hy Yee as or * RG bites € - —~7 , . | SOW TTTDAE Ean eee amatthaw yan tha aaa ceacaptteeesaetee TT NYT Doar : eet eettr ar enone ae if + 5 Ae he i a Pree Wy : ante of Mey ES ited 4 se Le ee 1 ht heed mee dilileht i ch eect MARL DTS ena Lhe LEN Ei) sod atm Dare Rw oe > Vurreue~ Vvurvw Mh 4 body ahve : ts pare. oe $ 4 4 cnt Pe Na x Te) Vues be ¥ 4) ; bee Tee ues : AAAS aa ' [ } dgi oak TR bab hdl wd» Maly wu as Nel wen Wiseun, | hike we egoaere® TTA Nth) NA et wo cayennnnt every «7 ey HTT TT oe “Fy ty, ce “* up Stay “CU pere oe 1 nate area { WU YN RE veer se rere’ a “1, \ y eH yet Ue. ‘Tl wie~ 5 hh fn rl Mdddar VFiy i ; A : a io Pel y A j my La ne On | wo , a Syren ay Ww i Sa am “K a oe t : ge! ay Oy Wy | wv i ST URUUTAHKTUN ITE Sv : - (Oy ee it Wh Wnt = § i i; ww SF C Pug er \y LT % Cty eee eT semi. oD sueceet j PPh Sin "4 fy ‘y,°an sof ysee cease see -* A dL AM prettonye, r] De he ny a wes - S0eunu = bh "on, id Ph he SEmaNrty | tent a bh heed ay for | i SO ee sia A ad HA ‘ivy Tt Wypyrevtti ddtoee ¢? yous ty yy ell dee die | Vw Me TT Mp yvee le ee Te Vevey cae Sg Ss it au bea iF “seerEMBER 1907 ‘York State Museum _ Joun M. Charke, Dice =; 7 < ot ae fey Bulletin. ss wo eer BY Wis H. P. CUSHING » tae toa eter 1 OPGSTapih ya fe ois nek oe PUeAever acs ws... 451 Gliciatione 20... 42° ss ot ae pees, tds. Mconomic=peology a... Sossg es: 502 Vteeets oct 45001: Pettasraphy- of the rocks. eka pee SOS Wane ons 404 Index... sre ees Ryman ss te bes SS oeO : a ALBANY. NEW YORK STATE EDUCATION DEPARTMENT ; ot yy Re i Recor eat S Price 25 cents ° STATE OF NEW YORK EDUCATION DEPARTMENT Regents of the University With years when terms expire 1913, WHITELAW REID M.A. LL.D. Chancellor - - - New York 1917 St Cuatrr McKetway M.A.LL.D.Vice Chancellor Brooklyn 1908 DanieL BeacuH Ph.D. LL.D: - - - - - = - Watkins 1914 Puiny T. Sexton LL.B. LE.D) - = = - == Baliye 1912 T. GuitrorpD SmirH M.A. CE“ LL.D. -.- > = Biteae 1918 WitLtiAM NotrincHamM M.A. Ph.D. LL.D. - - Syracuse 1910 Cares A. GARDINER Ph.D. L.H.D.LL.D. D.C.L. New York | I9I15 ALBERT VANDER VEER M.D. M.A. Ph.D. LL.D. Albany 1911 Epwarp LautersAcH M.A. LL.D. - - - - - New York — 1909 EUGENE A. Puirpin LL.B. LL.D. - - = =) = Neweiiams 1916 Lucian L. SHEDDEN LL.B. - - - - - - - Plattsburg Commissioner of Education ANDREW S. Draper LL.B. LL.D. ; Assistant Commissioners Howarp J. Rocers M.A. LL.D. First Assistant Epwarp J. Goopwin Lit.D. L.H.D. Second Assistant Aueustus SS. Downine M.A. Pd:D. LL.D. Third Assistant Secretary to the Commissioner Haran H. Horner B.A. Director of State Library Epwin H. AnpgerRson M.A. Director of Science and State Museum Joun M. Crarxe.Ph, Dy bi»: Chiefs of Divisions Accounts, W1LL1AM Mason Attendance, James D. SULLIVAN Educational Extension, Witt1am R. Eastman M.A. M.L.S. Examinations, CHARLES F. WHEELOCK B.S. LL.D. Inspections, FRANK H. Woop M.A. Law, THomas E, Frnecan M.A. School Libraries, Cuarues E. Fitcu L.H.D. Statistics, Hrram C. Case Visual Instruction, DELANcEY M. Eris e 7 :) - s 7 | maa es eo > ‘ PCS ee ee ee es ee heer EO ee ea ee eae ee ee eee New York State Education Department Science Division, October 19, 1906 communicate herewith, for publication as a bulletin useum, an account of the geology of the Adirondack as the Long Lake quadrangle accompanied by a on the scale of r mile to the inch, both of which ared by Prof. H. P. Cushing. Very respectfully Joun M. CLARKE ag Director 9 publication this 20th day of October 1906 New York State Education Department ee New York State Museum Joun M. Cuarke, Director Bulletin I15 GEOLOGY 14 GEOLOGY OF THE LONG LAKE QUADRAN GLE BY H. P. CUSHING ACKNOWLEDGMENT A portion of the field work, on which the following report is based, was done in conjunction with the topographers of the United States Geological Survey, while they were mapping the district. In country of this kind, where accurate location of out- crops is by no means the least of the difficulties under which the geologist labors, combined work of the sort is highly advantageous, since the topographer locates the geologist’s outcrops for him, and that with a high degree of accuracy. The arrangement was _ highly advantageous to the State Museum, as well as to the writer, and he wishes to express his hearty acknowledgments to Mr H. M. Wilson, whose permission made the arrangement possible, and to Mr J. M. Whitman jr, and Mr A. P. Meade jr, for a vast number of courtesies, and a very helpful and pleasant field season. SITUATION~ AND CHARACTER The Long Lake quadrangle comprises that part of the Adirondack region lying between parallels 44° and 44°15’n. latitude, and merid- ians 74° 15’ and 74° 30’ w. longitude, its area being slightly over 218 square miles. If the Adirondack region is understood to comprise _ the entire district of the north woods, then this quadrangle lies | about midway, or in the heart of the district. It is however situ- - ated on the western border of the more rugged portion of the area, that included in the Adirondack mountains proper. The quadrangle is noteworthy for the variety of topography presented. The main axis of elevation of the region crosses it, 451 452 NEW YORK STATE MUSEUM and its eastern border hugs the western edge of the high Adiron- dacks, the Santanoni quadrangle, just east, being one of the loftiest, most rugged, and most unsettled of the whole region. The southern border of the depressed “‘ lake belt’ shows well in the northern part of the quadrangle. The northern and southern halves of the Adirondack region are of somewhat different topographic char- acter, great igneous rock masses predominating in the former, and gneisses of various kinds in the latter, and the line of division between the two crosses the quadrangle from east to west about midway. The differences however are not as prominently brought out in the sketching, as they appear in the field. The Raquette, one of the greatest of the Adirondack streams, runs across the quadrangle, Long lake being merely a somewhat widened and perhaps deepened portion of the strearn, which enters it at one end and leaves it at the other. The great reach from Raquette falls to Piercefield, not far beyond the map limits to the west, is the longest possessed by any Adirondack stream. The rapids at Raquette falls are the only interruption to naviga- tion on the river which are found within the map limits. The quadrangle is also nicely illustrative of the number and variety of the Adirondack lakes and ponds, 57 of which are found, in whole or in part, within its borders. Threeof the larger lakes of the region, Big Tupper, Upper Saranac and Long lakes, are shown in part, somewhat over half the length, and all the wider part of Long lake being included. Of those wholly within the area of the map, Follensby pond is the largest, followed in order by Catlin lake, and Big Simons and Jenkins ponds, with thence a regular downward gradation to ponds so small as to make little showing on a map of this scale. In elevation of mean water level they range from the 1534 feet of Big Tupper and Big Simons, to the 2050 feet of Seward pond. Some of them are rock bound, in whole or part, with frequent rock islands; others have low shores of morainic material or of sand. Many of these latter are exceed- ingly shallow and are being rapidly converted into marshes. The extent of this conversion is well brought out on the map in several instances, as in the case of Pickwacket pond, in the extreme southeast portion of the quadrangle, and of Pickerel pond, 2 miles* south of east of Axton. The Tupper Lake reservoir is simply a dredged out portion of what was a nearly marsh-filled lake basin. With its frequent lakes, the long. reach of the Raquette river GEOLOGY OF THE LONG LAKE QUADRANGLE 453 with its bordering swamps and cut-off oxbows, the broad belt of low- land separating the highlands of the north from those of the south part of the quadrangle, and the difference in character of those two highland areas, the quadrangle shows a diversity of topography rather unusual, even for an Adirondack map sheet. Practically the entire area was forest covered until recently, and most of itis yet thus covered, though with a sadly changed forest. The rapid growth of the village of Tupper Lake, especially as a lumber center, has resulted in a steady increase in the amount of cleared land in its vicinity, and within the past 15 years the removal of the timber from the district has been rapid. The ordi- nary wasteful lumbering of the conifers (and much of the lumbering in the district has been of that type) is bad enough. But in addi- tion a vast amount of small wood for paper pulp has. recently been cut, and also much hard wood, so that there is now a wide area in the northern part of the quadrangle and thence north- ward for many miles, which has been practically deforested, and through which the great forest fires of May 1904 ran widely. Here as elsewhere, the Adirondack forest is disappearing, and much of it disappearing in such-wise that reforestation will be a difficult, if not impossivle matter. GENERAL GEOLOGY With the exception of the very recent, unconsolidated surface deposits, all the rocks found within the limits of the quadrangle are of Precambric age, or belong to the oldest known, great rock group. The length of that part of the earth’s history which these rocks record is not known, either absolutely or relatively, but it is known that the lapse of time involved is exceedingly great. and it is quite probable that 50% or more of the entire geologic history of the earth is included. Furthermore most of the Adiron- dack rocks are of early Precambric age, or were formed during the first half of this long time interval. They are hence to be classed as among the earliest of the known rocks of the earth. There are at least four great groups of these Precambric rocks, and their relations to one another are, for the most part, known. Unquestionably these groups are more or less capable of minor subdivision, but comparatively slight progress has yet been made in this direction. The study and interpretation of the history which these rocks imperfectly record is a matter of extreme diffi- culty, because the rocks have been profoundly modified, both 454 NEW YORK STATE MUSEUM texturally and structurally, by action of great compressive forces, so much so that many of them have lost all trace of their original character. These four groups are. t A series of old sedimentary rocks, the Grenville series, much involved with igneous rocks some of which seem of approximately the same age. 2 A series of gneisses which seem to be mainly or wholly of igneous origin, which may be, in part, older than the Grenville rocks, though no certain evidence of this has yet been forthcoming in the Adirondack region. If there are in the region any exposed rocks more ancient than the Grenville rocks, they are here. 3 A series of igneous rocks, usually in great masses (batholites), which are demonstrably younger than both the preceding, and which are not so profoundly changed in character, retaining often traces of their original textures and structures. 4 A series of very much younger igneous rocks which have under- gone little change since their intrusion. Rocks belonging to all four of these groups are found within the area of the Long Lake quadrangle, and all but the last have an ex- tensive representation, the quadrangle being rather unusual in this respect. . Grenville series. Here are classed certain wel! banded gneisses and schists, some of them very quartzose and grading into quartz- ites, with bands of varying thickness of coarsely crystalline lime- stone. They are believed to be old water-deposited rocks, ancient sheets of sand, mud and calcareous mud deposited on the floor of some large body of shallow water, in all probability the sea. There is apparently a great thickness of these rocks, but neither their base nor summit is known, and they are so disturbed, and usually so poorly exposed that our ideas concerning their thickness are of the vaguest. They must-have been deposited upon a floor of older rocks, but we are at present ignorant as to what these rocks were, and whether or not they are anywhere exposed in the district. Because of the thickness and the frequent changes in the char- acter of the deposit it is certain that the deposition of these rocks took a long time, pointing to a protracted submergence of the area at this early day, with frequent relative oscillations of the land and water levels. The close association of igneous rocks with them, some at least of which seem only found in this association, is thought to point to closely contemporaneous igneous action on a large scale. ‘ GEOLOGY OF THE LONG LAKE QUADRANGLE 455 Doubtful gneisses. Here are classed other rocks, differing from the preceding in that they seem to be wholly of igneous origin. They have been equally, if not more, changed from their original condition than have the rocks of the preceding group, and all traces of their original characters have disappeared. Similar rocks, in general not to be distinguished from them, occur associated with the sediments, where they are clearly as young, or younger than they are. So these may represent great masses of such rocks, massed in such amount as to have wholly displaced the sediments. On the other hand they may be, in part, older and represent the rocks of the floor on which the sediments were deposited. The question is, as yet, undecided; the former is the more probable. Great igneous intrusions. The rocks of the two preceding series at present found in the district constitute only a fragmentary rem- nant of those formed at this early time. They have suffered large loss from above by surface wear, slow but long continued. They have likely also suffered loss from beneath owing to the attack of masses of igneous rocks which were working their way upward. Prior to the appearance of these intrusions the older rocks seem to have suffered compression and as a result to have been much changed in character. At the time of compression they must have been buried under a considerable load of overlying rock, the great masses of the intrusions solidified under large load, and both are now at the surface because of the removal of this overlying rock during long ages of surface erosion. The intrusive rocks invaded the entire district, but Essex and southern Franklin counties felt the full force of the invasion, these igneous rocks forming most of the present surface there, while elsewhere they are not as prominent. These igneous rocks may be grouped into four great classes, anor- thosites, syenites, granites and gabbros, all no doubt derived from some great parent molten mass beneath by some process of dif- ferentiation. The anorthosite intrusion was the first and bulkiest, forms the heart of the igneous district, and was followed by smaller and more scattered intrusions of syenite, of granite and of gabbro. These rocks have also been profoundly modified by the action of great compressive forces, while deeply buried, but are not so thor- oughly changed in character as the earlier rocks, retaining many traces of their original structures. Following this time of igneous intrusion the region seems to have been a land area for long ages and to have undergone a prodigious 456 NEW YORK STATE MUSEUM amount of surface wear during the interval. The thickness of rock removed is purely conjectural but must have been large, several thousand feet at least. Later igneous rocks. Toward the close of this long erosion period came another time of igneous activity in the region, molten rock ascending toward the surface, and utilizing a system of east-west fissures for its ascent. Such lava-filled fissures are known as dikes, and such dikes are very numerous in the northeastern Adirondack region, though rather uncommon in the district under considera- tion. There was likely volcanic action at the surface, but this can only be conjectured since no known vestige of that surface now remains, all having. been since worn away. The source of the ma- terial is equally conjectural, though quite likely the same as that whence the great intrusions sprang. At the present surface we see only the old, lava-filled channels of ascent. Erosion still continuing after the close of the igneous activity, the surface was still further lowered, but by an amount to be meas- ured in hundreds rather than thousands of feet, the character of the dike rocks clearly indicating that they solidified at no great depth. Paleozoic submergence. Around the borders of the Adirondack region we find, resting upon the Precambric rocks, a series of sandstones, limestones and shales of early Paleozoic age, the Pots- dam sandstone of Cambric age beneath, and above in order the Beekmantown dolomites and limestone, the Chazy, Lowville, Black River and Trenton limestones, and the Utica shale, all of Lower Siluric age. In the heart of the region such rocks are wholly absent, save as scattered glacial boulders. Yet nothing is more certain than that they formerly extended over much of, if not over the entire, Adirondacks. When the submergence beneath the waters of the sea began, the region had been worn down to a comparatively smooth surface by long-continued erosion, and seems to have had a low, domelike summit in the present south- western part of the region, whence it sloped gently away on all sides. The encroachment of the sea was not steady but in oscil- latory fashion, but was in general progressive; in other words the waters of the successive seas usually covered a larger part of the yome than their predecessors had done. This was especially true jin the northeastern part of the district. Where we today find the Paleozoic rocks we can be sure that the sea was present, but since ‘ GEOLOGY OF THE LONG LAKE QUADRANGLE 457 they have been worn away from most of the region, the extent of the various seas is highly conjectural. It is quite unlikely that deposits of Potsdam age were ever laid down within the area of the Long Lake quadrangle. But the Beekmantown waters may have reached the district, it is quite likely that the Chazy waters did, and that deposits of Trenton and Utica age were laid down here is highly probable. The thickness which such deposits may have attained here can only be guessed at, but may well have amounted to several hundred feet. Subsequent history. At the close of the Lower Siluric the sea disappeared from the region and there is no evidence that it has since been submerged. It has instead been a land area, its sur- face undergoing wear. The altitude above the sea has however been changed from time to time, and whenever it has been increased, greater capacity has been given to the eroding agents. Many mil- lions of years have passed since the close of Lower Siluric time, no one can say just how many, and in that time every vestige of the deposits of that age has disappeared from the surface of the quadrangle, and the Precambric rocks beneath have also been eroded somewhat. What thickness of these rocks has thus been worn away can not be told, but many hundreds of feet seem to have thus disappeared from the hilltops, and from 1000 to 2000 feet more from the valleys. This is a considerable erosion, but apparently of much less magnitude than the great Precambric erosion. At the close of the Paleozoic occurred the greatest of the Post- cambric disturbances of the region. Great lines of fracture were formed, along which slipping, or faulting, of the rocks took place, along with much minor cross faulting. The great faults have a north to northeast course across the district, dividing it into a great series of slices. The cross faults more or less break these up into blocks of varying size, and at various levels. Some slight fold- ing of the rocks also took place, but of very minor amount in com- parison with the sharp folding in the New England area to the eastward, and the main displacement of the district was by fault- ing. Nearly all of the great faults downthrow to the east, produc- ing a rude, steplike drop from the central area down to the Cham- plain valley. To the eastward, in New England, folds, and large faults which downthrow to the west, occur, resulting in the great down-faulted trough of the valley. In the Long lake area and thence ™ 458 NEW YORK STATE MUSEUM westward, faults are not so prominent as to the east, and the general altitude diminishes in that direction. There was a minor period of igneous activity, in all probability of this date, which affected the country east and north from the Champlain valley, but not greatly to the west, and no rocks of this date are known in the area of the quadrangle. The general result of this period of disturbance was to considerably increase the altitude of the interior region. . A long period of comparative stability of level seems to have followed, sufficientiy long to have permitted of the wearing down of the whole region to a rather uniform, low altitude,.broad valleys with rather low, insignificant divides constituting most of the surface. Numerous hills were however left, with altitudes often several hundred feet above the general level. Following this a general increase in altitude occurred, greatest along the present main axis of elevation, and with likely renewed slipping along the faults on the Champlain side of the axis. The uplift renewed the cutting power of the streams and they excavated the present valleys of the region, the hills representing remaining portions of the pre- vious surface. No doubt many minor changes occurred during this long period, but as mere episodes in comparison with the two greater movements. Then followed the recent period of cold,and of ice advance over the region. How many advances and retreats of the ice sheet occurred across the Adirondacks can not be told, since the last advance obliterated all traces of its predecessors, at least no traces of them have yet been discerned. The ice plainly covered the region to a depth sufficient to submerge even the highest hill tops, and persisted for a considerable time. It did a respectable amount of erosion, and, when retreating, covered the country unevenly with glacial deposits. On its final disappearance it left the topogra- phy modified somewhat, owing both to wear and to deposit, but with its larger topographic features little changed. Ridge slopes were smoothed, summits rounded, valleys clogged with deposit, lakes produced either by inequality of deposit or by local excessive downward erosion, stream courses more or less modified, a host of . minor changes in detail, much altering the general appearance of the region. At the time of final disappearance of the ice the region had an altitude somewhat lower than at present, the amount in the quad- ‘\ « GEOLOGY OF THE LONG LAKE QUADRANGLE | 459 rangle being some 400 feet in all probability. The altitude has since slowly increased to its present amount, and the upward move- ment may yet be in progress.? ROCKS With the exception of the glacial deposits and boulders, and later stream and lake accumulations, all the surface exposures occurring in the quadrangle exhibit crystalline rocks of Precambric age. These comprise not only considerable belts of the sedimentary Grenville rocks, and great batholitic masses of anorthosites, syenites, granites and gabbros, considerably younger than and intrusive into the Grenville rocks, but also large areas of gneisses, which seem for the most part igneous, which can not yet be classified, but which are, at least in part, older than the great intrusions. Grenville rocks. The most extensive belt of Grenville rocks occurring within the quadrangle’s area has its broad northern end penetrated by the upper part of Follensby pond, down whose shores it runs for ? mile, with greatest breadth on the west side. It ex- tends southward from Follensby to the Moose creek valley, curving toward the southwest as it approaches it, and extends up this valley and its continuation, the Bog stream valley, to the west edge of the quadrangle.? Asit runs westit narrows to a breadth of less than a mule, which is less than half the average breadth south from Fol- lensby. _ This will hereafter be referred to as the Moose creek belt. Another considerable belt of Grenville rocks runs west and north- west from Round island, in Long lake, past Rock pond and Grampus lake to the quadrangle edge, with an outlying small area to the ‘ south running west from Grampus lake. No trace of undoubted Grenville rocks could be discovered on the east shore of Long lake, opposite Round island, doubtful gneisses constituting that district. This will be called the Rock pond belt. A third belt is crossed by the Raquette river just below Long lake, and extends up Cold river some 24 miles. This very likely extends down the Raquette to a connection with the Moose creek belt, but lack of outcrops in the interval save for a few meager exposures of doubtful igneous gneisses, renders the matter uncertain. This is the Cold river belt. There is a considerable area of Grenville rocks about the lower i For a fuller account of the geologic history of the region see N, ¥, State Mua, Bul, 93. Pp, 272-94. aSee accompanying map, 460 NEW YORK STATE MUSEUM end of Lake Catlin in the extreme southeast part of the quadrangle. This is likely a northward spur of the great Grenville belt which Kemp has mapped as running east for miles along the Long Lake- Newcomb road, in the Newcomb quadrangle which corners the Long Lake quadrangle on the southeast. At the time Kemp’s map was made only the actual limestones and closely associated schists were being included in the Grenville, whereas these rocks are quartz gneisses." On the Tupper Lake quadrangle, next west of the Long Lake, there is again at least one great belt of Grenville rocks, as yet unmapped, for numerous exposures of these rocks appear for several miles along that part of the Long Lake-Long Lake West road which lies between Little Tupper lake and the railroad. In addition to these belts there are several patches of varying extent of Grenville rocks occurring within the quadrangle limits, and such as have been recognized are indicated upon the accom- panying map. As usual, most of the Grenville country is valley country, owing to the weakness of these rocks as compared with the other crystal- lines. In general the outcrops are infrequent, scattered and poorly exposed, so that little or nothing can be done toward de- ciphering the stratigraphy, or.the structure. It is certain that the rocks are considerably folded, and also that the folds pitch, causing frequent changes in the direction of strike. The quartz gneisses form an exception to the general rule. “ Where present in consider- able thickness, as they are about the lower end of Lake Catlin, they constitute respectable hills, several hundred feet in hight, on the sides of which exposures abound. These quartz gneisses, or schists, constitute a prominent feature in the Grenville series of the quadrangle. They are metamorphosed sandstones of varying degrees of purity, and occur in part in beds of large thickness and fairly uniform character, and in part in com- paratively thin beds, alternating with beds of mica gneiss and of impure limestone. These latter quartz schists are much more variable in character than are the thick ones. In general the rock is rather evenly granular, though there are all gradations between a sugary, granuiar, weak rock, and hard, solid, glassy quartzites. In many instances thin layers of coarse, solid quartz alternate with the granular layers, and may comprise upward of half the tN. Y. State Geol, r7¢th An, Rep’t. Map opposite p. sso. 5 GEOLOGY OF THE LONG LAKE QUADRANGLE 461 whole mass. They are however a much more prominent feature of the thinner, variable beds, than of the large masses. All these rocks are very quartzose, but all contain feldspars in respectable amount. There are two main types of the rock min- eralogically. In one a light-colored pyroxene (a white or light green diopside) is a prominent constituent, while mica (usually phlogopite) if present is subordinate; in the other the pyroxene is subordinate or fails, and mica assumes much greater prominence. The pyroxene rocks are much more apt to be granular and weakly resistant to wear, while the mica rocks are comparable to many of the igneous gneisses in resisting power, hence their ten- dency to form hills. Much of the rock strongly resembles quite pure quartzite, but careful inspection always shows a considerable feldspar or pyroxene content. The larger number of the Grenville exposures in the district show a quite varying set of rocks in comparatively thin layers. The quartz pyroxene gneisses described above constitute an important feature. There are frequent, thin, micaceous bands in which, in addition to the mica, there is increased pyroxene and feldspar, and much diminished quartz, and which would seem to represent thin shale bands. Equally frequent are basic bands of hornblende mica gneiss, with black pyroxene and soda-lime feldspars for the other constituents, which have thus the mineralogy of gabbros, but are distinctly interbanded with the sediments. Rather thin bands of limestone occur frequently, generally quite impure, showing more or less pyroxene, titanite and graphite, grading often into border rocks of black, heavy character and composed chiefly of pyroxene. These limestones are interbanded with, and grade into the quartz pyroxene gneisses, producing all sorts of intermediate rocks, so that the series as a whole seems made up of alternate limestones and sandstone bands, with an occasional thin layer of shale. Exposures au not suffice to determine whether thick lime- stone masses are, or are not present. Ophicalcite was found in one single locality in the Moose creek belt. This general group of rocks is the one represented at the majority of the Grenville exposures of the quadrangle. Next to it in importance is the heavy quartzite group. No sillimanite gneiss was encountered, which is surprising, but not infrequently considerable masses of gneiss, both acid and basic, all cut up by quartz veins, and with frequent bands of solid quartz are met, which look sedimentary but are somewhat doubtful 462 NEW YORK STATE MUSEUM since in composition they are close to some igneous rocks. But their banded character, and the occasional appearance of thin bands which are quite certainly sedimentary, strongly suggest a sedi- mentary character for the whole. Such gneisses occur in force in the Moose creek belt, along Bog river. The garnetiferous gneisses, both acid and basic, which usually play sucha large role in the Grenville make little show in the district, though occurring in small amount here and there. The Grenville rocks are all cut up by other rocks which seem igneous. Some of these are plainly to be classified with the later great intrusions; but others are quite unlike these. Of these last some resemble phases of the gneisses here classed as doubtful, and shortly to be described, while yet others seem to be peculiar to the Grenville association and not to be found elsewhere. Yet their discrimination is a matter of great difficulty, there are so many phases of the other rocks to be borne in mind. Further their sup- posed diagnostic characters are much easier to recognize than to describe. Some rocks which seem quite certainly igneous are often apparently interbanded with the sediments, and may represent heavily metamorphosed contemporaneous sheets, or flows, or even beds of volcanicash. Other rocks which are unquestionably igneous, cut the sediments, and yet have not so far been certainly recognized away from the Grenville association. While indisputably later than the rocks which they cut, they are thought to be not greatly younger, and to be much older than the big intrusions. Yet the whole question is an exceedingly difficult one, and the poor and sparse rock exposures of the Grenville throw little light upon it. Some of these rocks have the composition, or at least the mineral- ogy, of granites, some of syenites, and some of gabbros. The latter are perhaps more apt to be distinctly interbedded with the sedi- ments than are the others, though all seem to have that occurrence at times. There seems considerable uniformity of structure in the different Grenville belts.. The general strike varies from west to northwest, and the usual dips are to the south and frequently high. In the Rock pond belt the strike varies between n. 30° w. and n. 60° w. in the Grampus lake vicinity, and from n. 60° w. to west nearer Long lake, hence has general parallelism with the trend of the belt. Inthe Moose creek belt the exposures are very poor and the dips are flat, so that it is difficult to get observations of any pretense to accuracy upon ‘ . GEOLOGY OF THE LONG LAKE QUADRANGLE 463 the strike. South from Follensby pond the rocks are much folded and with a general northwest strike, and south dip, but with much variation in both. This is in sharp contrast with the prevailing and usually high south dips in the Rock pond belt. The high dips occasionally run up to verticality and become steep north, sug- gesting the truncated tops of closed folds, but the north dip never persists very far. The Follensby Grenville is plainly cut out along the strike by the syenites which lie to the west, as would be expected from their proved intrusive character and later date. Along Cold river the strike varies from n. 25° w. to n. 50° w. in the few exposures, with a general dip of 45° s., though with much variation and plainly much folding. This strike is very suggestive of the extension of this belt to the northwest to a connection with the Moose creek belt, the proof of which can not be furnished owing to lack of exposures. | About Lake Catlin the strike varies from n. 80° w. to n. 60° w. and the dip is again to the south, and usually under 25°. West of the lake the sediments are much involved with gneisses apparently igneous, which soon cut them out entirely. On the hill in the extreme southeast corner of the quadrangle there is a thickness of close to 500 feet of the quartz gneiss exposed. No order of rock succession involving the different members of the Grenville could be made out anywhere, and but the vaguest ideas concerning the thickness could be obtained. In addition to the quartz gneiss thickness just quoted, a thickness of at least 200 feet of quartz pyroxene gneiss and impure limestone is shown on the low hill just south of Rock pond. But these are mere local details of what is certainly a great and thick rock series. Doubtful gneisses. These rocks divide themselves into two main groups: in the one we find comparatively uniform igneous gneisses without sedimentary admixture; in the other frequent bands or patches of Grenville rocks, and also frequent rocks of doubtful nature but with a Grenville look, appear, associated with the igneous gneisses. The first group will be styled for convenience the ‘‘ Long lake gneiss’ and the second “the Grampus egneiss.’”’ The edge of another great mass of these rocks appears in the extreme north- west part of the quadrangle, and extends widely westward. This will be called the “ Piercefield gneiss.” Long lake gneiss. This occupies a large area in the southern half of the quadrangle on both sides of Long lake, constituting the 464 NEW YORK STATE MUSEUM usual rock which borders the Grenville belts. The exposures ex- hibit a fairly uniform mass of gneiss, uniform in that it has a certain facies which is readily recognizable. It is not uniform in composi- tion, since it varies from a red, granitic gneiss to a black, gabbroic one, both kinds occurring in many exposures. But the bulk of the gneiss consists of these two sharply contrasted rock varieties. Frequent intermediate varieties occur, and the granitic gneiss shows considerable minor variation; but the group as a whole consists of alternating masses of granitic and gabbroic gneiss. The granitic gneisses show a twofold facies; most commonly they are finely and evenly granular and quite gneissoid; but mingled with these are many masses of quite coarse, granitic make-up, vastly less gneissoid than the other. In a few cases very quartzose granites of the Morris type, shortly to be described, occur, and they distinctly cut the other and are therefore younger. But in the majority of instances no such relationship is observable, and the distinct impression is created that the one rock is merely a phase © of the other; or in other words that the coarse material differs from the fine merely in having localiy escaped the excessive granulation which that has experienced. A red to brown feldspar is always much the most prominent con- stituent of this rock, comprising from 60 per cent to 80 per cent of the whole.t Quartz forms on the average from 15 per cent to 20 per cent, but runs both higher and lower. Black mica (biotite) is the next mineral in importance, though usually accompanied and frequently wholly replaced by hornblende. Both the granites and the granitic gneiss have essentially the same composition, though the latter are usually richer in the black, ferro-magnesian minerals. Black, amphibolitic gneisses constitute from 20 per cent to 30 per cent of the general mass of the Long lake gneiss. Sometimes they occur in bands only a few feet in thickness with red gneisses above and below, and here they usually appear interbanded, or in other words the contacts are parallel with the general foliation of the mass. From these smaller bands there are all gradations up to very thick masses of large areal extent.. For the most part these are hornblende feldspar gneisses, or amphibolites, the feldspar being mainly plagioclase, ranging from andesin to basic labra- 1 The mineralogy of this and the succeeding rocks will be described in detail in a later portion of this report. " GEOLOGY OF. THE LONG LAKE QUADRANGLE - 465 dorite. They range from fine grained, heavy, resistant rocks, to coarse, well foliated masses with conspicuous platy hornblende, which are weakly resistant and easily decayed. In the former type there is apt to be considerable pyroxene in addition to the horn- blende. In the latter black mica is pretty sure to develop, some- times in considerable quantity, assisting the platy hornblende in the development of well marked foliation. In many cases rocks, distinctly intermediate in character be- tween these amphibolites and the granitic gneisses, have been observed. In no case have they been seen to acquire large bulk, and in no case has it been possible to definitely determine their relationships. But since the amphibolites seem at times to shade into the granites through intermediate rocks of the sort, it is quite likely that we are dealing with impregnation of one rock by the other, with the effect disguised and equalized by the subsequent metamorphism. In all cases where these amphibolites occur in considerable masses, comparatively unmetamorphosed cores are found which show typi- cal gabbro (hyperite) as the original rock. All such found have been mapped as gabbro, both the unchanged core and the sur- rounding amphibolite being included. In the case of the smaller masses such definite evidence of origin is lacking, and all such have been included in the general mass of the gneiss. Yet they seem quite certainly to represent the same rock, in the one case only partly, in the other wholly converted into amphibolite by meta- morphism. A very accessible mass of such amphibolite is that composing the island toward the lower end of Long lake on which the Island House stands. It does not run into gabbro anywhere within the limits of the island, though it may do so under the waters of the lake near by. On all near-by points on the lake shore the granitic gneisses appear. ; For the most part then the Long lake gneiss consists of two sharply contrasted varieties of gneiss, both of which are unques- tionably of igneous origin. There then arises the question as to their age relations to each other, and to the other igneous rocks of ‘the quadrangle. It may be stated in the first place that small masses of similar rocks are found involved with the Grenville sediments, and ap- parently cutting them intrusively. So far as it goes this implies their later age, but in the uncertainty prevailing as to the equiva- 466 NEW YORK STATE MUSEUM lence of these small masses with the main one it is unsafe to say that the latter is younger than the Grenville, though it is quite likely. On the other hand if there are any rocks in the district older than the Grenville they are here. The gabbro of the unmetamorphosed cores is exceedingly like the gabbro found elsewhere cutting the anorthosite and syenite, and regarded as the latest member of the general eruptive series. This latter is often somewhat metamorphosed, but its metamorphosed phases show about the same mineralogy as the unaffected rock, though recrystallized into a granular rock, and do not run out into amphibolites, so far as the writer’s observation goes. The meta- morphism of the one seems less profound and of a different type from that of the other. The writer has never found these amphi- bolitic gabbros in connection with the great intrusives, never ex-— cept in association with the granitic gneisses, the Grenville rocks possibly excepted. The difference may perhaps be accounted for on the supposition that the inclosing granitic gneisses were less ~ effective as a protecting buttress against the stresses producing metamorphism, than were the massive and bulky anorthosites and syenites. And while this may be true and the two gabbros, not- withstanding their differences, be of the same age, it seems a much less likely supposition than that the one gabbro is much older than the other and its more profound metamorphism thus to be ac- counted for. Within the limits of the quadrangle no satisfactory evidence re- specting the relative ages of the two main constituents of the Long lake gneiss, the granite and the gabbro, has been discovered. Else- where in the Adirondacks however the writer has found amphi- bolites, in all respects like those produced from the gabbro by meta- morphism, distinctly cut by granites very similar to, if not identical with, these granitic gneisses, indicating that the gabbro is older than the granite. Since there is some question as to the precise identity of each of the rocks concerned, it is not safe to theorize too widely. It does however indicate the presence of a gabbro in the region older than a granite, both of which have suffered intense metamorphism; and hence enforces caution respecting the tendency to class all gabbros together because they are gabbros, and all granites because they are granites. While in doubt regarding these Long lake gabbros the writer is disposed to regard them as alder than the anorthosite, hence distinct from the later gabbro, ‘ GEOLOGY OF THE LONG LAKE QUADRANGLE 467 There is the further question, involved with the last, whether the granitic gneiss is a member of the general eruptive series, or is a considerably older eruptive. In part it is to be classed as a granite rather than a granitic gneiss, and this granitic portion may be younger than the rest or may represent less metamorphosed cores of the gneiss, analogous to the gabbro cores of the amphibolite. There is certainly some younger granite in the mass, but the im- pression given is that most of it is not separable from the gneiss and is simply a less metamorphosed phase of it. Ogilvie has recently described from the Paradox Lake quad- rangle, a gneiss which has many features in common with this granitic Long lake gneiss, if indeed it be not identical with it, and regards it as a granite belonging to the general intrusive group and younger than the anorthosite and syenite.t That there is a con- siderable body of granite in the region of which this is true, the writer is firmly convinced. But he is equally convinced that there is much granitic gneiss in the region which is much older than the anorthosite, and his present disposition is to refer the Long lake gneiss in the main to that group. It would vastly simplify geologic work in the region if Ogilvie’s interpretation of the Paradox granite could be shown to be generally applicable to the granitic gneisses of the district; but there are difficulties in the way. The anortho- sites and syenites contain not infrequently gneiss inclusions, some- times of amphibolite, and sometimes granite. These are unques- tionably older than the intrusives. Now there are amphibolites and granites associated with the Grenville rocks and the uncertain matter is whether these inclusions are from such rocks, or not. If not they distinctly point to the presence of older bodies of such rocks other than those associated with the Grenville; or else to large bodies of such rocks of which minor offshoots cut the Gren- ville rocks. The writer has not yet. obtained any evidence in the region which satisfactorily clears up these points. So the mapping of these rocks as gneiss is merely a makeshift, indicative of lack of exact knowledge respecting their age. Grampus gneiss. In the southwestern part of the quadrangle is a mass of gneiss which differs materially from the Long lake gneiss in the considerable diversity shown. It is in association with the Grampus Grenville and shows frequent patches of Gren- ville sediments of various kinds, which are too small to map on IN. Y. State Mus. Bul. 96, p. 484 et seq. ° 468 NEW YORK STATE MUSEUM this scale. There are various other gneisses present which are un- like anything found in the Long lake gneiss, except in the near vicinity of Grenville belts, most of which seem igneous, though some are of doubtful origin. Some of these gneisses are easily recog- nizable, others are discriminated from the Long lake gneiss only with difficulty. Along with all these is a general matrix of Long lake gneiss. -There is, for example, much of a black and white gneiss, which consists of hornblende or pyroxene and plagioclase feldspar, either andesin or labradorite, with accessory apatite, magnetite, titanite and zircon. In most of the occurrences the feldspar predominates, and the rock is spotted in appearance and fine grained. With increasing hornbleide the grain becomes coarser and the rock is striped instead of spotted. Often one variety is interbanded with the other. A similarly appearing rock in the field shows pyroxene instead of hornblende, with much titanite and a more acid feldspar (oligoclase). These rocks have the mineralogy of gabbros and dio- rites, but the field appearance is often suggestive of a sedimentary origin. There is often a strong resemblance to the rock of the “Whiteface” region which Kemp has described as the ‘‘ White- face type’ of anorthosite.t That rock behaves at times like an intrusive, at others strongly suggests a sediment, and its true nature and relations have not been clearly made out. If an igneous rock, its customary Grenville association has not been explained, and a close association in age is indicated; an age older than that of the ordinary anorthosite. Another gneiss in this group is a red, usually acid, rock composed of quartz and alkali feldspar, with a considerable content of green pyroxene and a deep colored titanite. This rock is also quite vari- able and is a frequent rock in the Adirondack region, often associated with magnetite deposits, as at Lyon Mountain. Its true nature, association and age are yet to'be discovered. There is also found much of a peculiar granitic rock, differing in appearance from the ordinary Long lake granitic gneiss, the dif- ference being difficult to describe, though easy to recognize. It is a rock of medium grain, not extra gneissoid, much lighter red than the Long lake gneiss, and contains from 10 per cent to 20 per cent of hornblende, magnetite and biotite. It occurs in a great number of Grenville sections, lying in among the sediments, or cutting them tN. ¥. State Geol. rsth An. Rep’t. 1895. . 587. GEOLOGY OF THE LONG LAKE QUADRANGLE 469 out, both above and below. It also occurs away from them in the general body of the gneiss. It may be a phase of the Long lake gneiss modified in appearance by the incorporation of Grenville material, but this seems unlikely, in view of its composition and it is tentatively regarded as a Grenville igneous rock, one whose in- jection took place during, or only shortly after, the deposition of that series. It is also thought that there are gabbros of similar age in the region, though no such have been identified within the quad- rangle limits. There are various other. varieties of gneiss found in the Grampus vicinity, though of very minor importance compared to those already enumerated. The whole mass is well banded, with frequent variations in composition and gives the impression of a Grenville area so intruded with igneous rocks of all kinds-and ages that the Grenville has well nigh disappeared, the whole subsequently exces- sively metamorphosed. In consideration of its complicated nature, and the trifling amount of certain sediments included, it is thought wiser to give it a noncommittal mapping than to map it separately from the Long lake gneiss. Piercefield gneiss. In the extreme northwest corner of the quadrangle there appears the eastern apex of a great mass of gneiss which lies mostly beyond the quadrangle limits, and which affords a somewhat different rock admixture from either of the foregoing. The rocks are excellently exposed about Piercefield, and in the railway cuts between Piercefield and Tupper Lake. These latter are on the edge of the main syenite mass, and show excellently two of the varieties of gneiss concerned, and their relations. These are a green, syenite gneiss and a red, granitic gneiss. The former is exceedingly like some of the very gneissoid phases of the syenite, near at hand. In one cut the red gneiss plainly shows an intrusive contact against the green; in another a pegmatite is at the contact, which repeatedly injects the green gneiss along the foliation planes. The pegmatite is a granite pegmatite, and seems to be a phase of the red gneiss. In both cases the green gneiss, which is quite horn- blendic everywhere, becomes excessively hornblendic near the ‘contact, and this is regarded as a contact phase of the green gneiss, though it is an unusual contact rock. Here is a syenite cut by a later granite, and a large mass of syenite near at hand. It would seem most probable that the two belong together, but they do not look alike, there are some differences in their mineralogy, and some 470 NEW YORK STATE MUSEUM slight differences in their chemical composition also. Much of the red gneiss is of the type which contains green pyroxene and deep colored titanite, like that described from the Grampus lake area, and sume of the green gneiss has the same minerals in abundance. There are also other gneisses present in minor quantity. It is quite likely that the green gneiss actually belongs with the main syenite mass, its differences being due to the granite intrusion. If so then in all probability most of the Long lake and Grampus gneiss should be classed with this granite as a great bulk of granite intrusive, later than the syenite, as Ogilvie has argued for the Paradox lake area. Owing however to the differences between the two rocks the writer hesitates to adopt this view without more decisive evidence, and has again taken refuge in noncommittal mapping. Great intrusions Anorthosite. A great mass of this rock lies in the northeast portion of the quadrangle and comprises about one fourth of its — area. It is but a small segment of a great batholite of the rock which has a wide extent in Essex and Franklin counties, and forms the larger part of the surface of the three quadrangles, Santanoni, Saranac and St Regis, which bound the Long Lake quadrangle . on the north and east. It repvresents the earliest of the great in- trusive masses which invaded the region in Postgrenville times. It is one of the most easily recognizable rocks of the Adirondacks, and its area is accurately mapped, so far as surface exposures will permit. This great mass of molten rock ascended to its present position and solidified, not at the surface but underneath a great thick- ness of overlying rock. This cover, and the upper part of the anorthosite itself, have since been removed by slow surface erosion. The present surface extent of the rock is simply the area of the original mass at the horizon where the present erosion surface cuts it. We can only conjecture as to its extension downward, though it no doubt runs deep and broadens downward. ‘The amount worn away from the surface is less conjectural. Sections © of the rock of above 3000 feet in thickness are exhibited in some of the mountains which it composes, suggesting the removal of at least that amount from the neighboring valleys, with an addi- tional unknown amount from the summits. This however necessi- tates the assumption that the original upper surface of the mass ‘ aSpoy orsny avou ‘Kr1v9 werpuy Aq saspoy aztsoyjyrouy De hae J GEOLCGY OF THE LONG LAKE QUADRANGLE 471 was comparatively even, which is far from likely. Near the present borders of the mass inclusions of the older rocks are found, suggest- ing that here we are near the actual upper limit. Since the rock was formed the mass has been much dislocated by faulting, shifting the relative levels of the old surface in the various fault blocks. This also urges caution in assuming that 3000 feet or more have been generally worn away from the valley regions, and also ren- ders it certain that quite different amounts have disappeared from the surfaces of the various fault blocks. If however the present surface were not far beneath the original surface it would seem that inclusions of older rocks should be more common than they are in most of the anorthosite district, and that we should also find downfaulted blocks of other rocks within it. So far as the writer is aware, such phenomena are mainly confined to the borders, and thus a quite respectable amount of wear from the upper surface is argued. The rock solidified as an exceedingly coarse porphyry, large crystals of labradorite feldspar, often several inches in length, abounding, surrounded by smaller crystals of the same material, for as a whole the rock is made up of this mineral, other constitu- ents being present only in very minor degree. The large crystals are of deep, blue-black color, often iridescent, and show bright, glistening cleavage faces, on which twinning striations are usually plainly observable. Originally the remainder of the rock was of _ the same color and in the least metamorphosed portions, when unweathered, it is today. Changes of composition are observable, both locally within the mass, and quite uniformly as its border is neared. These con- sist in increase in amount of the other rock constituents, with corresponding diminution of the feldspar. This may continue until they equal the feldspar in amount, and in exceptional cases exceed it, but these are extreme phases and one rock slowly grades into the other. These other minerals are augite and titaniferous magnetite, which are present everywhere in the rock in small quantity, and hornblende, hypersthene and garnet, which are not everywhere present, but are universal in the less feldspathic portions. Chalcopyrite is a widespread constituent, though in small quantity. The garnet commonly forms zonally around the magnetite, separating it from the feldspar, and the black center with the red zone of garnet surrounding it is a very common 472 NEW YORK STATE MUSEUM feature of the rock containing these constituents. Most of the anorthosite of the quadrangle contains garnet and the black min- erals in noticeable quantity, owing to its comparative nearness to the border. Like the other Precambric rocks the anorthosite has been much metamorphosed, being crushed or granulated and some- what recrystallized. But owing to its original very coarse texture, and to the fact that granulation mostly commences at the edges of crystals and slowly works its way inward, the rock does not appear so thoroughly metamorphosed as do the other rocks, none of which approached it in original coarseness of grain. The crush- ing which would have completely granulated a more finely crys- talline rock would only partially destroy the large labradorite crystals, and uncrushed cores of large or medium size would remain, even in the most excessively metamorphosed portions of the rock. With increase in the amount of dark minerals present the original grain of the rock seems to have been progressively less coarse and such rock is generally more completely granulated, with the uncrushed feldspar cores fewer in number and of smaller dimensions. This is a more common rock within the quadrangle than the coarser and purer variety. In some portions of the rock the feldspar crystals are more numerous, are smaller and are all arranged with their long axes parallel. This is a “flow structure’’ due to movement in the mass during solidification, which has strung out the already formed crystals into parallel arrangement. The granulated portion of the rock varies in appearance accord ing to the fineness of the crushing. In the majority of instances where not too finely granular, it has a grayish green to grayish blue tinge weathering to brownish. In more severely mashed portions the grain is very fine, gray to white is the color, the rock is very dense and hard, and uncrushed crystals much less frequent and of smaller size. Sometimes locally, either near bodies of later intrusives, or else in badly sheared portions of the rock, the feld- spar has been largely altered to a dull, white or greenish white material known as saussurite. This is quite different material from the soft products of surface decay of the same mineral. Rock of this sort makes up the rock point on the east bank of the Raquette * mile below the Raquette Falls landing. Similar material oecurs at various places in the woods. river 5 GEOLOGY OF THE LONG LAKE QUADRANGLE 473 Gabbro border of the anorthosite. The gradual change in com- position outlined above continues until, as an extreme product, a rock is obtained in which the heavy, dark colored minerals equal or exceed the feldspar in amount. A steady diminution in coarse- ness of texture accompanies this change, the uncrushed fe!dspar cores become continually smaller and less numerous till they finally disappear, and foliation becomes more and more promi- nent, so that the final product of the change is a heavy, dark col- ored gneiss which. bears no resemblance whatever to the normal anorthosite, and would not be recognized as a variant of that rock by an observer who met it for the first time, coming upon it from without the anorthosite area. If approached from the other side however the steady change from one rock into the other is plainly manifest. This final rock is not anorthosite but gabbro, and the rock intermediate between the two may be called anortho- site gabbro. It is perfectly evident from the field relations that this border phase of the anorthosite was produced by some proc- ess of differentiation in the general mass of igneous material after it had reached its present resting place, prior to or during solidification. For the larger part of its extent across the quadrangle the syenite, to be next described, adjoins the anorthosite, and a moment’s in- spection of the geologic map makes it evident that it has encroached upon, and cut out the anorthosite border to some extent. Between Follensby pond and the Raquette is a considerable mass of syenite which cuts out nearly the whole of the gabbroic border locally, and holds great inclusions of it likewise. In the Tupper Lake vicin- ity also the anorthosite has been badly cut out by syenite, and here again much of the gabbro border has disappeared. Outside the limits of the quadrangle there are localities where the gabbro border is lacking where its nonappearance is clearly owing to faulting. It is quite likely that originally the entire anorthosite area was characterized by such a differentiation border. In addition to this border differentiation to gabbro, a similar change has also taken place here and there within the general anor- thosite mass. A prominent area of the sort occurs near Panther pond, within a mile of Upper Saranac lake, which has been mapped as -gabbro. As it is approached the anorthosite becomes rapidly more gabbroic, but at the same time dikes of gabbro appear, cutting the anorthosite and in regard to the gabbro center it is not certain - t 474 NEW YORK STATE MUSEUM whether it should be classed with the anorthosite or with the gab- bro dikes. But these latter do not seem to be greatly younger than the general mass, and quite likely represent the injection of a’ por- tion of the mass which had already solidified by material from a yet liquid portion. Within the Santanoni quadrangle, next east, local differentiation has produced the masses of titaniferous iron ore of the Lake Sanford and Lake Henderson region.! These are well within the anorthosite mass with quite pure anorthosite for the general wall rock, and are remarkable for the narrowness of the gradation zone. No such masses, large or small, have been noted within the Long Lake quadrangle. This border gabbro is a rather uniform grained rock, of sufficient coarseness so that the white of the feldspar, the red of the garnet, and the black of the pyroxene, hornblende and magnetite are all prominent. In the less extreme phases of the rock, occasional small uncrushed feldspar cores remain. But the small, glittering, lath-shaped feldspars which are prominent in the less metamor- phosed portions of the gabbros associated with the Long lake gneiss have not been noted in this border rock, and the distinction is believed to be characteristic of the two rocks. Anorthosite outliers. Three small outlying masses of anortho- site have been noted within the limits of the quadrangle, and doubt- less there are others which have been missed, or which are covered by glacial deposits. Only masses rather remote from the main body are here under consideration. Curiously all three are in Litchfield park. They are from 4 to 7 miles distant from the main mass, with an intervening broad belt of Grenville rocks. To account for their presence here, and their nonappearance elsewhere is a difficult problem. In but one case do the exposures suffice to give any clue to their relationships to the surrounding rocks. The more northerly of the three outliers forms the summit of a small hill which lies between Jenkins and Long ponds. The hill breaks down quite steeply on the north and west in bare rock cliffs, was burned over some years ago, and second growth has not yet gained a foothold on the bare rock, so that exposures are excellent. The hill also forms an easily accessible and excellent viewpoint in all directions but eastward. In going north to the hill from the road between Jenkins and 1Kemp, J. F U.S. Geol. Sur: roth An: Rep’t, pt 3, DP. 409-17. GEOLOGY OF THE LONG LAKE QUADRANGLE 475 Long ponds, the rock at first is the granitic phase of the syenite, cut by dikes of fine grained red granite. This is shortly replaced by a variable rock which seems clearly a basic phase of the ordinary syenite, also cut by the red granite. At the extreme top is the anorthosite, extending about 300 yards in a northeast-southwest direction. The rock is quite typical, is medium grained, and labra- dorite feldspar constitutes 95% of it, magnetite, augite, chalcopy- rite and apatite being the other minerals. Not only is the passage from the syenite to the anorthosite abrupt, but in addition the latter is all cut up by dikes of the former, both large and small. It is also cut by dikes of the same red granite as that found cutting the previous rocks. On its northwest side the anorthosite is cut out by a reddish syenite whose relations to the main syenite are not absolutely certain, though if it be not identical it is a closely related rock. Red granite again occurs cutting both the other rocks. The anor- thosite is badly cut up by them and has been much altered in ap- pearance, likely by the heat and gases given off by the invading molten rock. The feldspar has been mostly converted to saussu- rite, producing a dull, white rock. This exposure, though small, is of much interest in that it clearly shows anorthosite cut by syenite, which is therefore younger, and granite cutting both the others and therefore youngest of all, the anorthosite being entirely surrounded by the other rocks, and there- fore an inclosure in them. A plausible explanation of its position, so remote from the main mass, and its inclosed situation in the later eruptives may be made by the following assumptions: that the anorthosite batholite originally extended to the locality, or else sent a large offshoot to it; that the later syenite invaded it and cut it out from beneath, sending out at the same time the big tongue of syenite which cuts out the anorthosite clear to the Raquette river; that the anorthosite inclusions indicate that the present surface is not far beneath the original upper surface of the syenite; that Grenville rocks originally overlay the whole, and have since been removed by erosion; and that later trough faulting dropped the block of Grenville that lies between, so that it has been less worn away, the syenite and anorthosite beneath still retaining a Gren- ville cover. though it has disappeared elsewhere. The second anorthosite outlier is near the county line (Franklin- Hamilton) 13 miles from the west edge of the quadrangle. On the 476 NEW YORK STATE MUSEUM south syenite gneiss adjoins it, and on the north granitic gneiss and amphibolite, similar to the Long lake gneiss. Unfortunately no contacts are exposed so that the interrelationships of the rocks are most uncertain. -Since the previous outlier proved to be an in- closure in later rocks it would be natural to regard this as probably a similar occurrence. The rock however differs-from the last, is much mashed, the feldspar shows wide variation in composition, especially considering the small size of the mass, and much scapo- lite has developed. It is not impossible that it may be a small out- lying intrusion, connecting beneath with the main mass, and with the syenite cutting it out on the south. The rapid changes in char- acter from place to place which it shows are more readily explicable on that supposition than if it is regarded as a small fragment de- tached from the main mass. But the whole question hangs upon the age of the granitic gneiss, and it is therefore doubly unfortunate that no contact appears. If the gneiss is older, this is a small separate intrusion, or branch from the main intrusion; if the gneiss is younger it is certainly an inclosure. The third outlier is upon the county line, 2 miles east of the sec- ond. It is completely surrounded by gneisses of uncertain nature and age, and no contacts are exposed. The rock is very gneissoid, no feldspar cores whatever remaining in much of it. It also holds from ro per cent to 20 per cent of minerals other than feldspar. The feldspar is an acid andesin instead of labradorite, being in this respect like some of the feldspar of the previous outlier. Both rocks are quite different from the ordinary anorthosite, while the rock from the first outlier is quite normal. This is but natural if the tw latter represent small intrusions into earlier rocks. Syenite. The general syenite of the Adirondacks has a much more irregular and patchy distribution than has the anorthosite, and the present day surface exposures belong to a series of separate masses both large and small. One of the greater of these masses, the Tupper syenite, has the larger part of its present surface within the quadrangle limits and, with the exception cf a few outlying in- trusions which are likely offshoots from it, is the only syenite mass within the quadrangle. It is separated into a smaller eastern; and a larger western portion by the Follensby Grenville. But if that lies in a downfaulted trough, as seems highly probable, the syenite may be legitimately regarded as continuous underneath, so that the separation into two masses is only apparent, and due to faulting. aIOYS dy} WO sqouy rvpIuis puv ‘aye, taddny, ur puvyst yoo. [[vws v Sururtoy oy1uads dJIGNV JO Sadpel payerovly a eit _ ; GEOLOGY OF THE LONG LAKE QUADRANGLE 477 The rock is exceedingly variable, much more so than is the anorthosite. Allthe varieties grade into one another, so that any separation in mapping is an arbitrary matter, necessitating the drawing of boundary lines where none exist. Yet the extreme variations are so unlike-the normal rock as to require separate rock names, and must be given a place upon the map, even at the cost of arbitrary boundaries. Normal syentte. This is a green to grayish green rock when fresh, with a rapid color change on exposure to the weather, assum- | ing a yellow-brown tinge and then becoming a rusty brown, the normal color on exposed surfaces. Over most of the district the weathered crust is not thick, and in any opening in the rock the normal green is quickly reached. It is a highly feldspathic rock, only second to the anorthosite in this respect, but carries from ro per cent to 20 per cent of other minerals, quartz, pyroxenes, hornblende and magnetite. Quartz never wholly fails, though not rising to large proportions in the normal rock. The pyroxenes are peculiar, and characteristic. The feldspar (microperthite) is of an entirely different nature from that of the anorthosite, is never iridescent, and does not show twinning striations on cleavage faces. The original rock was not so universally porphyritic as was the anorthosite, was seldom coarsely so, and even where coarsest was not comparable to the anorthosite in that respect. Hence, though the two rocks have experienced substantially equivalent meta- morphism, the syenite has mostly been mashed by the process, uncrushed feldspar cores being very few and very small in com- parison with the anorthosite. They are generally present in the normal rock however. For this reason the syenite has a more gneissoid look, and an appearance of greater metamorphism which is deceptive. The variations of the rock are in two main directions. In the one case the dark colored minerals increase in quantity at the expense of the feldspar, garnet appears, and quartz diminishes and disappears. The syenite passes into a monzonite and ulti- mately into a shonkinite. The rock also becomes more even grained and gneissoid, as does the anorthosite in its similar vari- ation. The more basic varieties have the dark minerals equaling or exceeding the feldspar in quantity and so strongly imitate the gabbro gneisses of the anorthosite border that they are exceed- ingly difficult to distinguish. In fact distinctly intermediate 478 NEW YORK STATE MUSEUM varieties appear, strongly suggesting that one rock has been modi- fied by incorporating material from the other. In the other direction the rock changes by increasing. quartz. The quartz also tends to appear in coarse leaves, or spindles, which are very prominent on the weathered surface or in the hand speci- men. The feldspar also changes slightly and tends to become red instead of green producing green and red mottled rocks. Finally the red predominates and the rock becomes a distinct granite. Basic syenite. This is in general a rather finely granular rock of general black color but sufficiently coarse so that the com- ponent minerals plainly show their proper colors to the eye. The feldspar is usually brown, though it is green where fresh material can be obtained. Garnet is in general not so prominent as in the gabbro, and the rock tends to a finer and more even grain, but the differences are slight. In general these basic rocks are con- fined to the near vicinity of the anorthosite, though in the ordi- nary syenite there is much variation from place to place in the percentage of dark colored minerals. It will be later shown that, even in thin section, it is very difficult to distinguish these rocks from the gabbros owing to the lack of distinctive features in the feldspars, but that chemically they are easily separable. Granitic syentte. As mapped this comprises a mass of very variable rock, much cut up by later granite, excellently exposed in Litchfield park and in the two big ridges which run north from it. Admirable exposures, often blasted, are found along the park roadways. Much of the rock is alternately green and red, quite quartzose, and a rock distinctly intermediate between syenite and granite, often passing into granite. Much of it is uniformly red, and the red rocks range from syenite to granite in composi- tion. It is not certain that all these latter rocks are of the same age, and differentiate in place of the main mass, and this is espe- cially true of the red syenite. But it is certain that much of the rock has this character, and the whole is manifestly bound to- gether as a mass of eruptive material arising from a common magma. It is all cut up by dikes and larger masses of a red granite, mostly too small to map separately, a rock to be shortly described as the Morris granite. Asymmetry of the syenite dtfferentiation. The formation of a gabbro border to the anorthosite by some not well understood process of differentiation, has keen seen to be a rather uniform yaed proyyoqy ‘puod suryuaf jo o10yYs yjiow / SIOP[NOd [VIoVpSs YIIM uUMaAzS ‘aq1uads-z}1enb par yo saspaT GEOLOGY OF THE LONG LAKE QUADRANGLE 479 feature of that rock. The syenite presents a sharp contrast in this respect, in that its differentiation is prominently asymmetric, and that, in the case of the Tupper syenite at least, this seems conditioned on the nature of the bordering rock. The most of the basic syenite, and all of the more gabbroic of it is in close asso- ciation with the anorthosite gabbro border; and the same feature is noted around the large anorthosite inclosures in the syenite. It is also true of the syenite bordering the anorthosite outlier in Litchfield park, this being the only basic syenite which occurs anywhere in the vicinity, so that its presence is especially sig- nificant. The differentiation into granite takes place on the south side of the mass, the bordering rock on the south being granitic Long lake gneiss. In each case the syenite grades into a rock approaching in character the adjacent rock. Now the syenite is unquestionably younger than the anorthosite, as will be immedi- ately shown, and the observed relations seem to point to the conclusion that the change is due to the actual digestion, by the molten syenite, of material from the adjacent gabbro. The rela- Ci OMe rile OlNer sides sare "not so’ “clea. “since” the sage of the bordering granitic gneiss there is unknown. If it be an older rock, as it is tentatively held to be, then the asymmetry of the syenite is certain. But if it should prove to be a younger granite then the view may be legitimately held that this granite has cut away a large part of the original syenite mass, thus account- ing for its apparent asymmetry. In consideration of the great amount of syenite that must be regarded as having disappeared on this hypothesis, however, it is vastly less probable than the other. In this connection it should be recalled that the Diana syenite, as described by Smyth, shows a quite similar asymmetric differentiation.t The character of the differentiation may thus be regarded as reasonably certain. The explanation to account for it, namely the incorporation of material from the adjoining rocks, is much more open to question. The syenite younger than the anorthosite. Reconnaissance work in this district in previous years had led the writer to believe the syenite to be younger than the anorthosite and the evidence then obtained was set forth.2 It was not however demonstrative, and as the matter is one of considerable importance in Adirondack Precambric geology, it was hoped that a detailed survey of the iN. Y. State Geol. 17th An. Rep’t. 1897. p. 471-86. aN, ¥, State Geol. aoth An. Rept, 1900, Dp, 741-544 480 NEW YORK STATE MUSEUM boundary between the two rocks. might furnish proof of its verity. This was in fact one of the principal reasons for the selection of this quadrangle for detailed study. The hope was fulfilled, the evidence being as decisive as could be desired. 3 About Raquette falls, on both sides of the river, anorthosite and syenite are found in mixed distribution. All exposures are in the woods, in no case was any contact observed, and it is only by the relative abundance and. distribution of the two rocks as brought out by the mapping that it is inferred that east of the river the syenite is present as small bosses or large dikes, - cutting the anorthosite, while west of it the anorthosite has been largely cut out and mostly occurs as inclosures in the syenite. The evidence given by the first. anorthosite outlier in Litch- field park has been already presented. The anorthosite is defi- nitely cut by syenite which sends dikes into it. The syenite is of the basic variety in part, and in part is reddish syenite; the whole is surrounded by a zone of mixed rocks, granitic syenite and granite which, though believed to be mostly a differentiation phase of the syenite, lies between it and the normal syenite farther north, preventing the definite tracing of one rock into the other. It is along the northern edge of the quadrangle, where the land has been cruelly lumbered of late years, where the great fire of May 1904 made a clean sweep of what was left, and where much of the land has since been cleared, that the decisive evi- dence was obtained. Even as far east as Upper Saranac lake occasional dikes are found cutting the anorthosite. These are narrow, the dike rock is fine grained and peculiar and of two main types. One is a hard, ringing, light colored, feldspathic rock, with frequent small garnets, but with other dark minerals present but sparingly. The other is a dark, heavy, gabbroic- looking rock, with abundant garnet. From its appearance in the field it might be either a gabbro or a basic syenite. Now while these rocks suggest syenite in appearance they differ much from the main body of the rock, which shows no similar phases. Yet it is obvious that the physical conditions under which they cooled differ so much from those under which the larger masses solidi- fied, that a considerable difference in appearance and character is normal, rather than abnormal. And the study of thin sections led to the confident belief that they were really dike offshoots from the main mass prior to the discovery of decisive field evidence. GEOLOGY OF THE LONG LAKE QUADRANGLE 481 The series of exposures that decisively settle the question occur along the Wawbeek road within the first 4 miles eastward from Tupper Lake. In the neighborhood of the village itself the rock is quite typical augite syenite, though with a tendency t) -become basic locally, well shown in the road metal quarry near Raquette pond, where the rock is very hornblendic and lacks feldspar augen [pl. 18]. The syenite runs eastward for about a mile, then for an equal distance there are no outcrops, after which they are numerous on both sides of the road, the best and most continuous being south of it, where exposures run with practical continuity for another mile. The rock is chiefly anorthosite, somewhat gabbroic, but by no means the normal border gabbro, Lan tm a mueain ui + + + Ft + See SS SST Sin Sy 2.88 anorthosite syenite dike syenite Fig. t Relationship of syenite and anorthosite, as shown in an exposure 2 miles northeast of Tupper Lake village, and not far south of the Wawbeek road. Scale r inch = 34 feet this,of itself suggesting that part of the mass has been cut away by the syenite. In addition it is everywhere cut through and.through by dikes of the syenite, both large and small, and in increasing number as the main syenite mass is neared. The wider dikes show a rock identical in all respects with the syenite about Tupper Lake, sometimes basic, at others not so, and there can be no question that they represent direct offshoots from the main intrusion, cutting into the anorthosite. From these larger dikes, composed of normal syenite, slender branches may be Seen running out into the anorthosite, and in these the rock is at once recognized as identical with that found in the more remote slender dikes, giving a demonstration of their origin, and cf the fact that they differ from the ordinary rock because of their. slenderness, and hence more rapid cooling. In figure 1 is given a 482 NEW YORK STATE MUSEUM sketch of a portion of one of these surface exposures, which shows the observed relations clearly. Just adjoining it on the east is an exposure which shows chiefly syenite, but with inclosed blocks of anorthosite. In these exposures neither of the two rocks has the extreme basic character of the usual border phase of each, though the syenite is more basic than the normal rock. Granite. Both the anorthosite and the syenite, especially the latter, are found cut by dikes and larger masses of granite. So far as the writer’s experience goes this granite is always of a single, easily recognized type which he has called the “ Morris granite,” from its frequent occurrence on Mount Morris, south of Tupper lake. This is a quite uniform, red, very acid granite, constituted almost wholly of red feldspar and quartz, other minerals being usually not visible to the eye. It presents both a fine grained and a coarse phase, the former being more common. The coarse type is especially distinctive because of the segregation of most of the quartz into coarse leaves or spindles, which are very prominent in both the weathered and unweathered rock, and stripe the red - feldspar with streaks of dark, glassy quartz. In the other and more common type the quartz shows as small, dark colored, glassy spots in the prevailing red of the yet finer grained feldspar. In some exposures the fine type appears as a border phase of the coarse and the coarse type has not been seen without the pres- ence of the other also. The fine type however frequently occurs without the other being present, the narrower dikes of the rock are always composed of it, and some of the larger ones also. The coarse is not only found grading into the fine, but also appears GING JON su The granite produced as an extreme phase of the syenite differ- entiation differs much from the Morris granite in appearance. It is usually coarse grained, though running locally into fine types, is quite hornblendic, and is not especially quartzose. The black blebs and streaks of hornblende distinguish it sharply from the Morris type. In the coarse varieties the quartz tends to.assume the leaf form, but the quartz is usually subordinate to the horn- blende in prominence. Varieties however do occur which are distinctly intermediate between the normal types. These two granites belong unmistakably to the general group of the later intrusives. Similar rocks are found here and there within the general body ef granitic gneisses of the region, But GEOLOGY OF THE LONG LAKE QUADRANGLE 483 their presence does not aid in the general solution of the problem as to the age of the bulk of this gneiss, since if it be older it would be apt to be cut, here and there, by outlying masses of the later eruptives. Such masses are frequently found in it, but in general the evidence does not permit the determination of their char- acter, whether they cut the gneiss or belong with it. Gabbro. The gabbros are dar': colored, basic rocks, usually showing a reddish tinge owing to tlie presence of garnet. As found within the quadrangle the rock occurs mainly in the dike form, and these dikes have been noted cutting all the other eruptives, with the exception of the granites, leaving the relative ages of the two somewhat in doubt though the granite is thought to be the older. In addition to the dikes is the small boss which cuts the anorthosite south of Panther pond. The rock for the most part is tough and resistant, and generally rather evenly granular. It lacks the gneissoid character of the gabbro border of the anorthosite, and weathers much less readily than that. It has not been noted grading into amphibolite, after the fashion of the gabbro found with the Long like gneiss. The smaller masses and the dikes of that rock are always found in the amphibolite ‘condition, and this more metamorphosed condition seems to argue a greater age, though it is possille to explain it as due to local causes. The unchanged cores of that gabbro have also a more pronounced ophitic structure than has been noted in this later gabbro, though that also tends toward the same structure in the larger masses. It is only with the greatest difficulty that the rock can be distinguished from that of the dikes of gabbroic syenite. This will be later reverted to. As a possible exception to the above statement the gabbro knob at the farm in Litchfield park, just west of Jenkins pond, must be instanced. This is thoroughly metamorphosed to a micaceous amphibolite, yet is an unquestioned gabbro; nevertheless it is entirely surrounded by granitic syenites, regarded as belonging to the later eruptives. Unfortunately no contacts show and the rela- tions between the two rocks can not therefore be made out. It would seem to be easiest accounted for on the assumption of a knob of later gabbro cutting the syenite. It is rather large for an in- closure in the syenite, yet the writer’s present disposition is to re- gard it as such, since the Long Lake gneiss is close at hand tu the south. Ifit be not, it of course vitiates the attempt made above to 484 NEW YORK STATE MUSEUM discriminate between the two gabbros on the basis of difference in character. Diabase. But two dikes of this rock have been noted within the quadrangle limits. The larger and more accessible of the two is on Round island, in Long lake, showing the usual dense, heavy, black rock with chilled borders and coarser center, and with occasional porphyritic feldspars. On the southeast edge of the island both contacts with Grenville rusty gneisses are exposed, showing the dike to be 30 feet wide and to bear n. 30° e., and that it is not vertical but dips 60° s. No fresh material could be obtained from the dike but it is one of the ordinary olivine diabases of the region. The other dike was noted on the south slope of an anorthosite - hill on the east edge of the quadrangle. Neither contact showed and there was but a single exposure so that its thickness and trend can not be stated. It is an ordinary nonporphyritic diabase. Two other similar dikes are known just west of the quadrangle limits on the Tupper lake sheet, and a few have been located on the compara- tively unexplored and rugged Santanoni quadrangle, just east. They are infrequent in the mid-Adirondack region, though abund- ant farther east. ROCK STRUCTURES ; Foliation.t The rocks of the northern half of the quadrangle are chiefly massive eruptive rocks, in which foliation is absent, or at best only rudely developed. This is mainly owing to their highly feldspathic character, and the scarcity of the minerals which are good producers of foliation. The gabbroic anorthosite and the basic syenite have it much better developed, and the tendency of the quartz to assume the leaf type is responsible for a poor foliation in some of the granites. Conspicuous foliation is only found in the Grenville rocks and portions of the Long lake, and Grampus @nelsses. In the Grenville sediments foliation and bedding correspond, in all cases in which it has been possible to determine their relation- ship. But the Grenville rocks cover such a comparatively small portion of the area, exposures are so infrequent and in general so poor, and the stratigraphy of the series is so little known, that scant idea of the general structure could be obtained from the usual methods. 1 Foliation is a convenient term for that variety of flow cleavage found in wholly crystal- line rocks, which have wholly or largely recrystallized under pressure, and which hence possess a parallel arrangement of mineral particles, resulting in a capacity to split more | readily in one direction than in any other, \ GEOLOGY OF THE LONG LAKE QUADRANGLE 485 In the Moose creek belt the dips are so flat that they can seldom be made out with certainty. Elsewhere the\V are higher, and in a few instances distinct folds are shown. These are ofthe sharply pinched, or closed type, steep south dips becoming vertical and then steep north. But north dips are exceptional. Such folds as show pitch show.it to the west or northwest, but it can seldom be made out. Since no aid could be obtained from the stratigraphy in decipher- ing the structure of the region, it was hoped that some light would be thrown on it by a careful plotting on the map of all the observa- tions on the foliation dip and strike [see map]. In many of the ex- posures only the strike can be made out, and this is notably the case in the poorly foliated eruptives. Even in the gneisses the foliation is often poor and indistinct, making exact observations difficult, and the whole result is indecisive and disappointing. Taking the quadrangle asa whole, nearly east and west strikes prevail, and the prevalent dip is southward. This either indicates comparatively little folding, or else isoclinal folding, or else that the foliation does not coincide with the bedding and so does not bring out the folding. It is not possible to demonstrate which of these alternatives is the true one, though the second is very unlikely, _and all the direct evidence obtainable is against the third. The south dips vary widely in amount, and there is certainly considerable local folding. In spite of the uncertain nature of the result, certain facts are brought out. The foliation is more erratic in the eruptives than in the gneisses and Grenville rocks. In the southeast the prevalence of east and west strikes and south dips is noteworthy. In the southwest the strike has swerved to an average n. 65° w. direction, the dip remaining south. Meridional strikes are exceptional and most frequent in the central portion of the quadrangle. Locally, on the northwest, north dips prevail. There is a local prevalence of northeast strikes about the foot of Long lake. The general nonfoliated character of the anorthosite is brought out by the absence of observations in the territory occu- pied by that rock. It is obvious that these observations must be extended over a wider area before their significance can be apprehended. Joints. The number of readings taken on joints within the ‘quadrangle limits is 647. When tabulated in respect to direction (all odd degree readings being reduced to the nearest 5° direction) ~ 486 NEW YORK STATE MUSEUM they are found to run in all possible directions [fig. 2]. In individual exposures the majority of the joints are seen to be curving instead of straight. This shows that some latitude in direction must be allowed each joint set, but is not decisive as to the amount of allow- ance necessary. Few exposures show more than two good sets of parallel joints, though some show three and even four. Certain compass directions are frequent in certain portions of the quad- rangle, and utterly fail elsewhere, indicating a shifting of direction, rather than a different joint set, it is thought. From the best ex- posures it can be learned that in general there are two sets of joint couples, each couple consisting of two sets of parallel joints which 123 t Fig. 2 Diagram of the readings on joints within the Long Lake quadrangle. The inner figures represent the compass degrees east and west of true north; the outer row the num- ber of joint readings observed for each 5° direction. Four numerical groups are also indicated. approximate a right angle with one another, and that one couple tends to occupy the meridional and equatorial directions, the othe running northeast and northwest. An attempt may be made to classify the entire number of readings on this basis, assuming that each set has a variation in direction of 20° owing to swerve. Thus then. 80° e. ton. 80° w. joints are grouped together, forming a couple’ with then. 10° e. to n. 10° w. joints; inlike manner the n. 40° e. to n. 60° e. and n. 30° w. to n. 50° w. joints are grouped. The numericat results of this grouping are indicated in the diagram, and a greater number of the readings are included, on this basis of subdivision, than on any other possible basis using the same amplitude of swerve. It is quite certain that some of the joints have a swerve of this amount, but it is not impossible that they may have even more. qyurof “Mm ob u ev Suope Suraq jjos}t sovy Ytpo ayy ‘s}urof Surmoys ‘ayuy soddn yz, S1¢ [ ‘pUv[st yUT_ Jo pus ysaay nos ye IPD GEOLOGY OF THE LONG LAKE QUADRANGLE 487 This grouping still leaves a large number of not included joint readings, especially in the n. 20° e. and n. 70° e. directions. This is either indicative of two additional sets of joint couples, a n. 20° Se tOrm7O> Wo and an. 70° €. to n. 20° w. couple, or else shows that the amplitude of swerve in the original couples is consider- ably more than 20°. Ifit be as great as 4o° the extreme directions of swerve of adjacent pairs would meet, or overlap. But it is very improbable that the amount is as great as this. If the region consists of faulted blocks, as is quite likely, and if the joints are older than the faults, also highly probable, then a reasonable and probable explanation of the apparent confusion would be furnished. Both hade and throw vary along faults, caus- ing some change in horizontal orientation in the various fault blocks, which may at times become considerable, and produce an equivalent shifting in the directions of preexisting joints. Hence the prevailing joints in adjacent fault blocks might well show a lack of accord in direction, thus accounting for the prevalence of certain joints in certain districts and their absence elsewhere. For example in the southwestern part of the quadrangle the more com- mon joint directions are n. 10° e. and n. 50° e., the latter set more variable in direction than the former. The set at right angles to the first is still more variable, from n. 80° e. to n. 80° w. in direc- tion, while the northwest set is most variable of all, and happens to be the strike joint set. In the southeast the n. 10° w. direction is the most prominent, there are no n. 10° e. joints and but one read- ing to n. 50° e., the two prominent directions in the southwest. The n. 80° e. to e. and w. direction is next in prominence and is the strike joint set. The northwest set is again very variable in direction. In the fairly massive eruptives, where there is little or no folia- tion, the joints are mainly highly inclined to vertical. Hades up to 20° from the vertical are common, especially in the curving joints. But there is often present a set of nearly horizontal joints, also quite irregular. i In the gneisses of the southern half of the quadrangle there is a joint set which is plainly dependent upon the foliation. This varies in general from a n. 80° e. toa n. 50° w. strike, and in many exposures good dip joints are seen whose strike is nearly or abso- - lutely identical with that of the foliation. There are seen also to 488 NEW YORK STATE MUSEUM be two sets of joints with this strike, a set of dip joints, dipping with the foliation which is to the south in general, and another set at right angles dipping north{see pl. 4]. These would seem quite certainly to be compression joints whose location was influenced by the foliation, but whether they antedate the vertical joints or not can not be told. Lines of excessive jointing are not infrequent in the eruptives. In such places from two to four joint sets are well marked, and the joints are closely spaced, their distance apart being measured in inches rather than feet, chopping up the rock into a multitude of small blocks, and forming prominent lines of weakness in it. Often multiple faulting has taken place along these strips on one of the joint sets, grinding and slickensiding the rock surfaces. This faulting seems to be of Precambric age, and has been noted in sey- eral places, affecting both the eruptives and the gneisses. The entire rock complex along the gorge at Raquette falls (gabbroid anorthosite cut by gabbro) is remarkably shattered by multiple jointing of this sort throughout the length of the gorge, a distance of nearly 1 mile. At the lower end the Sheared joints run n. 10° e., but elsewhere the trend is n. 40°-50° e., and no n. Io° e. joints appear. The trend of the gorge is clearly determined throughout by this joint set. There are also two sets of inclined joints, strik- ing n. 50° w., one hading 20° n., the other 45° s._ It is exceedingly probable that considerable faulting has taken place on the north- east joints. Many excellent examples of the same sort are shown in the fine series of exposures along the roads in Litchfield park in the granites and granitic syenites. By the road along the north shore _ of Duck lake, about midway of the lake, occurs the most shattered material seen in the quadrangle. The rock is granitic syenite, cut . by Morris granite. The slipping has been along an. 65° e. joint set, so closely spaced as to form an excellent fracture cleavage, .con- siderable secondary quartz has been deposited, and the rock rap- idly weathers down to a mass of fine splinters, strongly resem- bling rotted wood splinters at a little distance, all due to excessive shattering, accompanied in all probability by faulting. Faults. It is not easy to demonstrate the presence of faults in districts whose stratigraphy has not been deciphered and to defi- nitely locate them and determine their magnitude, in such areas, is well nigh impossible. It is however known that faults are fre- Near view of the steep south face of the Mt Morris spur. The cliff rises quite sheer for some 800 feet and is probably a fault scarp GEOLOGY OF THE LONG LAKE QUADRANGLE 489 quent and important structural features in the Paleozoic rocks which fringe the Adirondacks; that they most abound on the east; that on the north and south they diminish in number and mag- nitude going westward, and that on the west they are small and infrequent. It is also known that they are normal faults with nearly vertical hade; that many of them have throws of several hundred feet (some of from’ tooo to 2000 feet); that the principal ones run north to northeast; that there are numerous cross faults running west to northwest; and that from the Paleozoics they run into the crystalline rocks with their magnitude unimpaired. A priori therefore their presence should be expected in the Adiron- dacks, and they should diminish in importance westward through the region. The Long Lake quadrangle is in the mid-Adirondack region. In the Mohawk valley large faults are found considerably west of its meridian, the Little Falls fault, longitude 74° 50’, being the most westerly of the large faults there, and with an average north- northeast trend. Faulting on that trend, prolonged into the Adi- rondacks from Little Falls would involve the Long lake region, and some evidence of faulting would naturally be expected, though not as prominently as would be the case farther east. - Actual evidence of faulting is furnished by the slickensided char- acter of the multiple joint surfaces previously described, but this seems to be faulting of very ancient date, and is not the common type of faulting here under consideration. The indirect evidence for faulting in the district is twofold. 1 Topographic. As repeatedly urged by Kemp for the more faulted district to the east the shape of the ridge blocks, a gentle crest slope in one direction and a steep cliff face in the other, is strongly suggestive of block faulting, and indeed no other reason- able explanation suggests itself for it. Fault scarps of the sort appear in the Long Lake quadrangle. The great cliff on the south side of Mt Morris [see the topographic map and pl. 5] is one such, and is one of the most conspicuous examples in the whole region. The two big ridges to the southeast of Mt Morris are also of the block- faulted type [pl. 19]. But on the whole this type of ridge is not especially prominent within the quadrangle, or at least recent faulting of the sort is not suggested outside of the examples men- tioned. Others of the ridges do somewhat suggest more eroded examples of the same type. : HOON dik NEW YORK STATE MUSEUM 2 Grenville belts and patches. To explain the situation of some of the Grenville rock belts, inclosed on both sides as they are by the later eruptives, it seems necessary to assume that they lie in downfaulted troughs. They now constitute valleys with the eruptives forming the adjoining ridges, as well as underlying the Grenville at an unknown depth in the valleys. This makes a con- siderable and quite abrupt change in the level of the upper surface of the eruptive. Unless these are downfaulted troughs it seems necessary to assume this curiously irregular upper surface to the igneous batholite, so that the other supposition seems vastly the more probable. The areal mapping seems to emphasize this suggestion, though the evidence has not the weight it would have in a district whose stratigraphy was well worked out. The boundary between the Follensby-Cold River Grenville and the anorthosite and syenite which adjoin it on the northeast, appears to be a fault contact, though the Grenville exposures are not frequent enough to enable exact mapping. The boundary between the Moose creek-Bog stream Grenville, and the syenite and gneisses to the north, is also suggestive of faulting. Too little is known of the relationships of the Grampus gneiss to warrant any deductions from the mapped contact between it and the Grampus Grenville. TOPOGRAPHY The main axis of elevation in northern New York bears south through western Clinton and Essex counties to the Marcy region, then swerves to a southwesterly trend which is continued through Hamilton county. This line forms the major axis of the Adiron- dack highland. From it the surface drops gently westward toward Lake Ontario and the St Lawrence; from it the surface drops more abruptly and jerkily eastward to Lake Champlain. The minor axis of elevation passes westward through Essex and southern Franklin counties, intersecting the other in the Mt Marcy region. The general highland of the northern half of the Long Lake quad- rangle constitutes the western portion of this minor axis, while the entire quadrangle lies west of the major axis. : In northern Hamilton two broad valley regions cross the major axis separating the Hamilton from the Essex portion. Oné of these valleys is certainly and the other probably located on a beit of Grenville rocks. The lowland along the southern margin of *yeotd Ay ayinb st aspa auo yw sutdy puod ay} ‘punorsar10y oy} ul Ad[[VA pvorq 9Y} puUv UMOYS ][OM SL $}Sor0 OSpra oy} Aq oats oury Ays uaad Ajaatyeivduios sy y, ‘aye~T oy} Jo xodv yynos dy} YoSnory) sassed sa1jzuUN0d OMY 9Y} WOOAMJoOq OUTT OYJ, “MATA prt oy} UL OVE Yond yw ‘Ajyunoo urpyuesy ‘yavd ppayyouy url yruums pry vw wrosy ‘Kyunoo uojzpiweypy oyut yynos SuryooyT GEOLOGY OF THE LONG LAKE QUADRANGLE 491 the Long Lake quadrangle constitutes the northern portion of the first of these lowland belts. A similar, though less conspicuous lowland belt is developed across the south center of the quad- rangle, again located on the Grenville rocks, and separating the two highland areas of the quadrangle. Peneplains. It has been elsewhere shown to be espaol that, during Mesozoic time, the Adirondack region was worn down to a comparatively even surface or peneplain, which was subsequently uplifted, and that the accordant levels of the hill and ridge tops and crests observable in the southern and western Adirondacks are due to the fact that they are remnants of this old ’surface.t The uplift renewed erosion and the present broad valleys of the region were cut out, the comparatively concordant levels of their bottoms marking the new base level, and their depth below the peneplain horizon measuring the amount of uplift. Since their development there has been further uplift of the region, the old valley bottom level is no longer the stream grade, and the streams are now engaged in the task of cutting down to the new grade, in which task they have made but slight progress. i All these uplifts have somewhat tilted the old peneplain sur- face though the amount of tilting is but slight, and in the southern and western regions the even sky line of the ridges is everywhere notable. But on the northeast the ridge tops appear at varying altitudes and hardly suggest a peneplain surface. This is thought to be due to renewed faulting during the more recent times of uplift, giving the various fault blocks differing altitudes, and destroying their previous concordance of surface. It seems also to be true that monadnocks, or parts of the old surface which were never worn down to the general peneplain level, are larger and more abundant in the vicinity of the main axis of elevation than they are elsewhere, and this makes an additional obstacle in the way of recognition of that surface. The probability that faulting has played some part in the production of the present topography of the district, though by no means as important a part as it has farther eastward, has already been indicated. Therefore more evidence of former pene- plaination should be observable here than there. An inspection IN. Y. State Mus. Bul. 95, p. 423-27; Ogilvie, I. H. N. Y. State Mus. Bul. 96, Pp. 468-69. 492 NEW YORK STATE MUSEUM of the topographic map shows that in both the northern and southern highland areas the hill summits tend to elevations of from 2600 to 2800 feet, with the Kempshall and Morris summits alone overtopping that elevation as small monadnocks [pl. 5, 6, r4]. A study of the topographic maps of the adjacent quadrangles how- ever quickly dispels the impression that we have here a peneplain level which can be shown to extend over any considerable area. On the St Regis quadrangle, just north, but a single hill (St Regis mt, 2882 feet) exceeds 2600 feet elevation, and there are but two others which reach 2500 feet, most of the hills ranging from 1900 to 2200 feet. There is further seen a range of hills running across the quadrangle from northeast to southwest east of which lies a depressed belt, the lake belt, in which the hilltops little exceed 1800 feet, yet the rock is anorthosite, as it is in the higher range to the west. This lake belt seems a downfaulted trough, and its southward prolongation forms the northwest portion of the Long Lake quadrangle. The altitudes of the hill range are fairly con- cordant with those of the highlands on the Long Lake quadrangle. In both the valley levels are near 1600 feet, indicating that the dislocation of the peneplain surface by faulting dates mainly from the time of the first uplift which followed. its formation. On the Santanoni quadrangle, adjoining the Long Lake on the east, there are several peaks over-4000 feet high, the main water- shed of the region appears, and we are carried at once into the high Adirondacks. There are no elevations concordant with those on the Long Lake sheet, and there are many things which suggest ' considerable faulting. Because of proximity to the watershed the valley levels are also higher, but seem fairly concordant, taking this into consideration. South, on the Blue Mountain quadrangle, are many peaks with altitudes well over 3000 feet, with Blue mountain, 3759 feet, overtopping them all. There are also many lower hills which are more in accord with the general Long lake altitudes. Whether the higher hills are to be classed with Kempshall and Morris as monadnocks, in which case they would be very numerous, or whether they represent the peneplain level, dislocated out of accord with the Long lake levels, is not certain. Topography as conditioned by the rocks. Owing to their weak resistance to erosion, in comparison with the other rocks of the region, the Grenville rocks give rise to valleys, and the main ‘ “‘JSOMYINOS 9Y} UO UIVJUNOU dq} SopVUTUTIA, Yor Yrpo eyy yo yavd aoddn oy. savaddy qouy yruuwmns oy} Jo 7Y S14 241 IV “[PA2] SLY} PAoqe qouy yIwuUNs ay} JO UOIVAITA JYSI[S 94} puv $}Ssoso oaSprt ayy Jo our AYs word ApAIvyz oY SUIMOYS JSAM YY WOLF SSVUL SILLOJ TN OU, ‘Aydvasodoy SJL OyVIISNI[L puv sstous ayevy Suo-y yo orv ILIV “OSNOTT PULTST oY} Wor] ‘soSpra SUIUAATAJUL ay} pure lvysdway yy 8 AeId I}ISOYjJIOuB jo 918 MOTTA 9} ul Sospti 9d T1V “SOUBISIP IVF oy] ur ulvjunOm puvssoduy yA ‘JJ2] 24} US yojou AOT[VA a}jonbey oy : YR Suo'y ‘asnoyzy PUBS] 94} Wory a8uvI preMmas oy, Ui ee GEOLOGY OF THE LONG LAKE QUADRANGLE - 493 valley belt of the quadrangle is a Grenville belt. Because of the greater strength of the quartzite member of the series, it gives rise to considerable hills in each of the belts, but otherwise they are low. It is quite likely, too, that the lowland along the southern margin of the sheet, and that about Round pond, is really Gren- ville territory. The few exposures seen in each area are of uncer- tain gneisses, and do not suffice to definitely determine what the prevailing underlying rock may be. Except for the lowland along the north margin of the sheet, which belongs to the lake belt.. and is likely due to down faulting, the main lowlands are owing to the presence of Grenville rocks and their weakness, The hills tend to the long ridge type with their major axes trending northeast-southwest. Those which suggest faulting have a northeast pitch to their crest, and a steep, clifflike back slope on the southwest, as seen on Mt Morris and on the ridges east of Little Simons pond. Stony Creek mountain shows an ap- proach to the same type. On the other hand the long, irregular ridge of Rock Pond and Grampus Lake mountains does not at all suggest the type, and the Kempshall mass is not even of the ridge type. There is a tendency on the part of the elevations in the gneiss country to be of the hill, rather than of the ridge type, as illustrated by Mt Kempshall and Buck mountain, while this type is practically absent in the anorthosite and syenite country [pl. 7-9]. Drainage lines. In so far as there are belts of weak Grenville rocks, the, valleys so located are drainage lines, whose trend is determined by that of the Grenville belt. Moose creek, Bog stream, lower Cold river, and the Raquette between Cold river and Moose creek, are the principal streams of the quadrangle occupying Grenville valleys. In so far as the remainder of the water courses are concerned, the lines of weakness which they occupy must be structural rather than stratigraphic, hence must be lines of joint- ing and faulting. Hobbs has recently presented strong arguments for the belief that such lines have had predominant influence in the location of the drainage lines of New England and Eastern New York.t Butitis difficult to apply the argument in a district where joints are found with all possible compass directions, as they are within this quadrangle. Yet, as has been pointed out, there are certain directions of more frequent, and more important IJour, Geol. s1g01. 9: 469-84; Geol. Soc. Am. Bul. 1904. 15: 483-506, 494 NEW YORK STATE MUSEUM jointing and it is of interest to ascertain whether those directions are also the more usual directions of the drainage channels. Since faults have not the prominence that they have to the eastward, they can not have the important effect upon the drainage that they there have. The two prominently linear drainage lines of the quadrangle are the Long lake, and the Raquette-Upper Saranac lines. The trend of Long lake throughout its 134 miles of length is closely n. 35° e., nearly half of the lake being on the Blue Mountain quadrangle. Above the lake the Raquette follows the same trend line for at least 2 miles more. Below the lake for a mile we have the Raquette and Cold rivers on the same line, beyond which Calkins creek follows it for 5 miles more; in other words for 21 miles this is a linear drainage line. Other lines, though shorter and less prominent, have the same trend; the line containing Rock pond, Second and Third Anthony ponds, and their inflowing creeks for one; Grampus and Handsome ponds and the main tributary to Upper Moose creek form another; the Raquette from the mouth of Moose creek to the landing below the falls is equally linear though not quite parallel, the direction being n. 45° e. This is the most prominent drainage direction in the southern half of the quadrangle. It is even more prominent to the southeastward, the Indian lake-Upper Hudson line having the same trend. * In the northern half of the quadrangle the meridional direction is the more conspicuous. The most prominent line of the sort is that followed by the Raquette river from the falls to Axton, then across to Upper Saranac lake, the valley being blocked by drift sands be- tween the two points. The lake, 74 miles long and trending north and south is on the same line. Follensby pond, with its inlet and outlet, and the Raquette river below as far as Tromblee’s, constitutes another such line. These straight courses would all seem to be determined by lines of jointing, and likely of multiple jointing and slip faulting. It is certainly true that the meridional joint direc- tion is the more important in the northern, and the northeast direction in the southern part of the quadrangle, and these drainage directions are in accord with this. The east and west direction for the tributary streams is the more common one in the district, though this prominence is vastly better brought out on the Blue Mountain quadrangle than on the Long Lake. Here the line of Ampersand brook and the Raquette river GEOLOGY OF THE LONG LAKE QUADRANGLE 495 from Axton to Follensby outlet is the most important one. The Bog stream and Big brook stream have the same alinement. The northwest direction is uncommon, though it becomes the prevail- ing stream direction in the quadrangles to the northwest. But in these the faulted. district has been left behind, and the streams seem to be consequent streams. GLACIATION Striae. The location and direction of the glacial striae noted within the quadrangle limits are indicated upon the accompanying map, with two additional readings just outside these limits to the west. All are found by roadsides, upon recently stripped ledges. But the larger number of the rock exposures elsewhere show glacial rounding and polish, the striae being obliterated by the weather. The fact that recently stripped exposures show them with great frequency, seems to indicate that they were abundantly produced within the district. Further, all seen are in valleys, and some of them in valleys whose trend is at right angles to the direction of ice motion. Ogilvie has urged that, in the high Adirondacks, glacia- tion was comparatively feeble and mainly effective upon the hill- tops, the ice in the valleys being comparatively stagnant.t But if this be true it can only be so for a very restricted area, since the Long Lake quadrangle closely adjoins the high district, and the valleys show abundant evidence of considerable glaciation. The 1o readings on striae shown on the map vary in direction from s. 25° w. tos. 75° w. While plainly influenced by the valley trends they harmonize well with the statements of Kemp and Ogilvie that the general direction of ice motion across the Adiron- dack region was a southwesterly one. Six of the 1o are in harmony with that statement. The other four, the two on the north shore of Jenkins pond, the one by Littie Simons, and one of those outside the sheet, are influenced by, and have closely the trend of the val- leys in which they lie. More striking instances of similar deflection are shown on the Tupper Lake quadrangle, next west, where, on stripped ledges along the railroad, readings of n. 80° w. and n. 75° w. were obtained, parallel to the trend of the Raquette valley. The general southwest direction also holds on that quadrangle, and there also striae are found numerously on recently stripped ledges. Glacial deposits. No heavy and thick deposits of till have been noted within the quadrangle limits, nor any bulky moraines. There I Jour. Geol. Apr. May r901. v.10; N. Y. State Mus. Bul. 96, p. 470. 496 _ NEW YORK STATE MUSEUM is however often a respectable amount of till, and many areas are at least thinly covered with morainic material. But on the whole glacial removal seems to have been in excess of glacial deposit. The main areas of morainic accumulation are shown on the ac- companying map, though not fully, only those sufficiently extensive to render the areal mapping somewhat uncertain being shown. It may be said in general that the main valleys all have their floors banked up with drift, and that the north slopes of the ridges are apt to be similarly encumbered: The matrix of the deposits is quite sandy, or gravelly, as is usual in the Adirondacks, but they contain many large boulders, and there are often large boulder trains on the surface. : A moraine of considerable prominence runs across the northern portion of the quadrangle from Tupper lake to Axton and bevond. There is a tendency to kame development along its front, as is common in the district, and at Moody is a notable instance of the sort [see map and pl. ro]. The waves of the lake have eaten away its end producing a 20 foot sand bluff, showing cross-bedded sands with a coarse gravel streak near the top. A short distance back it runs up to a conical summit, 150 feet above the lake. Yet further east it runs up against the moraine, two flat terraces appearing. during this rise, their surface covered with gravel and occasional cobbles, but no large boulders. This fringe of water-laid material borders the moraine on the south for a considerable distance. About Tupper Lake Junction is another development of sands, and Little Wolf pond, whose southern shore appears at the north margin of the sheet, is held up at the south by these sands. A great sand . and gravel terrace, with occasional large boulders extends up the Cold river valley, banked up against the anorthosite hills beyond, and seems a true kame terrace. The broad Grenville valley belt of the quadrangle is rather heavily moraine covered. The local character of the drift is empha- sized here since Grenville boulders abound, but elsewhere are scarce or absent, so that they can be used rather confidently for areal mapping. Throughout the gneissic area also the low grounds and the gentle hill slopes are moraine covered. The accumulations are in general not large, nor do they tend prominently to the ridge type. _ There is no indication within the quadrangle limits of any pro- tracted pause during the ice withdrawal. Numerous cuts in till are shown along many of the roads, espe- Bluff produced in kame sand ridge at Moody, Tupper Lake shore. Cross-bedding shows midway at the top. GEOLOGY OF THE LONG LAKE QUADRANGLE 497 cially in the northern half of the quadrangle. It is quite sandy or gravelly in character, and has been much used for surfacing the roads, answering fairly well for that purpose in many places. Valley plains and pitted plains. In the district north of the Long Lake quadrangle there is evidence of pause in the ice retreat, in the considerable moraine which runs west from Placid to Saranac, and thence on northwest to Lake Clear and Brandon. Running south- west from this is a great sand-filled valley, commencing at Lake Clear and ending at Tupper Lake Junction. The general character _ of its surface is well shown on the St Regis quadrangle topographic map. A number of small rock knobs project above it, and the rail- way cuts west of Saranac Inn station well illustrate the general way in which these knobs are wholly or partly drowned in the sand. The material is mostly even grained sand of medium grain. There is little gravel in it and no clay. . In addition to the rock knobs the surface shows diversity of another sort, small oval or circular depressions below the general surface which are in some cases dry and in others occupied by small ponds. There is a notable collection of these between Upper Saranac lake and Lake Clear, and thence northward to Upper St Regis lake and beyond. It is exceptional that a topo- graphic map brings out the feature better. The general area is also noteworthy in the number of lakes and ponds. There are about 150 of these in the St Regis quad- rangle, in all probability a greater number than is found on any other of the Adirondack map sheets. And they are mainly massed along this sand belt and occupy depressions in its surface. The upper end of Upper Saranac lake has these sands for its shores, and the abundant and good sized ponds to the westward have also sandy shores except for the occasional rock knobs protruding through the sand. The general level of the deposit falls to the southwest though the fall is only slight, from 12 to 18 inches to the mile. The sand must have been deposited from a current which ran across the region to the Raquette just below Raquette pond. In order to account for this flow we must presume that. the present outflow through the Saranac river was blocked, and it would seem that it must have been blocked by ice which lay near at hand. The depressions in the sand are of the kettle hole type, and the fact that the larger ponds were not filled by the sand suggests that they were occupied by stagnant and slowlv melting ice tongues 408 NEW YORK STATE MUSEUM which persisted until after the melting back of the main ice front withdrew the water supply from this particular channel. The sub: sequent disappearance of the ice tongues left the basins occupied by the present ponds. The small kettle holes were likely formed in the same way, small unmelted ice masses being left during the general retreat of the front, covered with sand and subsequently slowly . melting away. The Upper Saranac lake valley was likely occupied by the largest tongue of all, and the sands were washed upon its north end but were otherwise kept out of the valley. If this be the true explanation of the character of the district it follows that the ice disappeared from it by melting back toward the northeast and that, for a time, the Raquette river carried the upper Saranac drainage: There is another and parallel line of identically the same nature on the St Regis quadrangle, extending from the Forestmere lakes down to Bay pond and beyond, with a tributary line coming into it from the north at Brandon. The sands are similar and the sur- face characters identical. The writer is not familiar with the dis- trict to the west and does not know whether a connection with the Raquette drainage can be traced or not. The flow may have been down the St Regis. There are two small sand-filled channels, one wholly and one partly on the Long lake sheet. The former extends from Coreys to. Axton, the route of the old Indian carry. The material is mainly sand though there are a few gravel streaks. A few surface boulders are to be seen, but very few. The surface partakes somewhat of the kame character and this was likely a channel of water dis- charge only during the time that the ice was retreating back over it. It is this sand filling which prevents the water of Upper Sara- nac lake from coming south to the Raquette river, to which drain- age it properly belongs, and sends it through the modern channel, over the rock ledge at the Saranac Club (Bartletts carry). The other channel comes down to the Raquette river at the oxbow 1° mile below Tromblee’s (not the Oxbow further downstream) and takes off from Upper Saranac lake at Gilpin bay. It seems also a local channel, used for a short time after the abandonment of the pre- vious one, and before the ice had withdrawn to the north of Upper Saranac lake, opening up the great channel decribed previously. Topography as modified by glacial erosion. The all pervading effect of glacial wear in the region was the rounding off, smoothing and polishing of the rock knobs, large and small [pl. 1-3]. Except ‘ ‘usa Myoq royvayyrydue daap v YA sands OM} yno Spulas pUv jSaMYINOS 9Y} UO 4NO Suapeorg yf "71 Seyvutrxordde yr YSnoyy addy oSpr4 peord dy ayy Jo JOU SI UTeJUNOUI dy J, ‘“soTIM HE JIwWUWNS OY} 0} 9dULISIG “jSVITJAIOU ySv9 SULYOO] ‘uo}XVy WorJ UvzUNOUM Yaery AU04S porveys pue pejutol 6 Shas week ee, TOs Se —— 35 O57 ZA COMM hoe ahiat erate ese nee enc ie meen 4x455) 2 oa 0.29 AD att OSS a ans: aie ene che See RIED == i = 0.10 Graphite as «ican Perch eaten GEO = —— 0.03 Total gees io tsk eee eae eee ee ee 2125 6130 IO0.00 Composition calculated from mode Qz. Pyrox. | Phlog. | Orth. Alb Anor. Tit Zir. & Ap.| Total SiO2.. 202A USs7S| Foyt Baoan O.07]| 2.23) Osi® ©.09| 68.09 JAN, Org etied crate 2 nO oy CaO ae osvall En Y/Alln cs ao bolloaa 6 45 Tieeiay IEA 2.30 Nici OS ers eee (Oye hae Mee Netra sig .09 (aac n || Belisch esc We Bidteoes|| aces oot TD Als CaQe Hea e cscs HWA XO} Sa MER pal Sha er Boel Malema ©.97| ©.16 ACG 5.66 Nias Olas sere teee OVE OsOSlo oso Tal | ays coeliac iene alle ee ihe 57 KO eee teas OPO? TAG MO OA Le saan ee [evteytmas niet peace eases B) Ai) Wine wo clloo.o ea Oye DT [ee 4S colic aeekeeeita | eae cavers & | Seer ermies oleae alle eae On fr Ope eteh irae rersicl ia etaterc || Ge RERe cota las Bacehenis Mer Iiepate eer ©) 22) nena 0.22 Lit Os. (callie ee eos Sal hestak es aU H awe e cectee | ne reece red vases |eier te eee | ee ©.20| 0.20 AD © Jena eared eine | anor asi ey eset | Miele oy elles Serine a Jct ceefeee eee ©. O23) OnOs Total... 3o.22) 34°56 (26ers!) eos so cOble Aeeaener sy ° 38) 99-97 ! what uncertain and its result is of itself pretty good evidence that the pyroxene is of quite different character from that analyzed and used in the calculation. The lime-magnesia ratio seems clearly quite erroneous. If the lime and magnesia percentages in the pyroxene calculation are reversed, bringing it more closely into line with the composition of ordinary diopside, this anomaly disappears. - “uwooq Soy, oy} Aq JouUUYO ULewW 9} Woy poyeavdas udaas st YOIYM pue ‘Moqxo IauIIOF v Jo UOTWISOd dy} SyIvUE YOIYM sYSnoys yasyovq oy} Jo 9uo dn Suryooy] ‘WO}XW JO JSAM SO[IUE ZUIYV] MITA “pIBMIS IJ PABMO} ASAI ayJonbey oy} Jo JauuvYyo ureut oy} ssotoe SuryooT oz 93eIg GEOLOGY OF THE LONG LAKE QUADRANGLE 509 As so modified the analysis falls closely into line with the preceding, though representing a much more impure sandstone, somewhat more shaly, and much more calcareous than the more quartzose rocks. It seems quite clearly a member of the same group. Just north of the Bog stream. near the west edge of the quad- rangle, quartz, pyroxene, feldspar gneisses occur which appear less distinctly like sediments in the field, and have somewhat the look of the ordinary gneisses. But portions of the mass are excessively quartzose, and in thin section all resemble the Grenville quartzites just described. The slide of one of the more quartzose portions shows a quartz, feldspar, pyroxene rock with small amounts of titanite, magnetite, apatite and zircon. Phlogopite is lacking, and the rock is firmer, more glassy looking and less granular than the usual quartzites. The microscopic analysis however shows a close relationship. Mode of quartzose (Grenville) gneiss (6-B-2-a) Units Units measured Sp. Gr. by weight % weight BO) Maisie a Se nen eed ee eke? eto 2ret x 2.65 == B7o0 == 65.78 INGICIs ores ese char A eid oee eanrere sae een oe A953 £205 == BOER == 23.00 JEN ROD AGNES Fk doer ata cat aR eae PORZ2 = Cor = 9.29 Bier er eit berminn. to, crecna tactausee ia we, ae -tkee ante 10% 3.5 = oo = 0.65 Mia sale tiveness Steno ce ee are TES 2 == 27 == 0.42 ANIDE HIMES sto cnehore Uae acneinee neue OOS een DEEZ = O = 0.07 AGC O Meare errant eene hem bea Saab GPS Se tas as. aa Sie — ©.10 MO Lellet ge. pavesey eis crete = wreceios wie ee 3183 8666 100.00 Composition calculated from mode Qz. Orth. Alb. Anor. | Pyrox. Tit. Mag. eee Total SiO. OF 73) 2.33) See 9 Ag) §.@4)"OsAolla co ce< 0.03] 85.18 Eel OR cas ale esses < GOS A Reni Sorell” Cz, SO) leeaisee creel agen exec oh le 6.20 ISAO) a trate fororaud cee ||Geeie cee || Sentoneieneh ianene Paes Opal letter OPN s oe dec 0.45 GO) ewer aaa ern et ne tak chat, By ©), ONG 658 ae (ope ae eer 0.76 NUEA OO erssoiseeil eyes ected cert seer ewepener ICN ere Deals skelter sus an eee TE «Wf Oe raat ecteas seal uch etd eon oie 's Perr eee || wa Ome O lectern OnOd| 5 3.12 BNO Pini Sexaisets arta war? ERAGE HA lo sciates ROO) Pas ners abet oi ees 1.50 ESO cal ee oe OOO eon eco ftrea che: ONS ONS Aces of Soave, erase eee mere 0.69 Jul al Oss Os AN tocedene bela Ra Ears Caer eneen ene OR OBI sees, Gece Bate teal terete iets 0.03 Li Pa rays eel ete creetell rsctra tee |scvanaueteltat|ieiGeenec rallies a =e o's SFA AO) | eer rails ciedotes 0.26 i One Ss Sia ioten 5 Coch Ge AEE tea a eRe RE ah hehe eee eee eel eect GO| O©.07 Nhe earliest eu te enoe seensll saya a lems cts ails ave stele atieels ©.02| 0.02 Total (Hs Fi BaGe)) 22 Oe) SECC) OLAOI o OAOH) Cave)" Ce milo woyey- Oy 510 ; NEW YORK STATE MUSEUM As usual some uncertainties have a vitiating effect on the calcula- tion. The pyroxene may, or may not be like the one analyzed. If not the lime-magnesia ratio would be altered, though the change would be slight. Most of thefeldspar is twinned, though 15% lacks - this feature. This has been calculated as orthoclase though it may not be. The remainder shows a maximum extinction of 16°. This is the angle for both albite and andesin (Ab, An.) but this is held with reasonable certainty to be the latter since Becke’s method shows it to have the same refractive index as the quartz. Except for a possible slight increase in lime and corresponding decrease in _ magnesia therefore this must give a very close approximation to the actual composition of the rock. It harmonizes well with the preceding analyses and again indicates a somewhat impure sand- stone, a little more aluminous and a little less calcareous than they. Igneous rocks. Granite. No analyses of the Adirondack gran- ites have been published, so far as the writer is aware. The Morris granite is of a distinct and simple type, with definitely established age relations to the other intrusives, and an accurate analysis of it seemed highly desirable. It is mainly a quartz-microperthite rock, with accessory plagioclase, hornblende (usually chloritized), mag- netite, titanite and zircon, and lends itself readily to microscopic analysis. Since however the character of the feldspar can not be precisely determined microscopically an analysis was necessary to establish this. The hornblende has been thoroughly altered to Mode of Morris granite, fine grained type (15-A-3) Units Units measured Sp. Gr. by weight % weight Qua REZ ea er VEE AE Hee ond eRe aaa Ox 2.65 == 2030 = 444557 Micropentiites a. sm timeanc Soom is IGM AG == AGO == O2,74 PlasiOclase =k. ee tees cane Ce I 22.63 = 153 = ook Elormblendestiie ocr eae sete a 30 = (88 Macnetite sce oe oe sone etme ie SRS = 2 = 0.34 ZAR COM orators shoe eae ee ese Pe B83 So SS 13 = o.18 Mat amibes see saaiks cis ois eieneaek eaten elas 13.5 = —— 0.03 Motel crs Get ca Se tecoe ss heb pein are 2856 7610 100.00 chlorite and small flecks of this mineral are frequent in the feldspar, and are too small to measure accurately, so that the hornblende should more properly read “ chlorite” and its amount is certainly GEOLOGY OF THE LONG LAKE QUADRANGLE Sir considerably too small. The amount of zircon is probably too . large, and the slide does not seem to show quite the normal amount of magnetite. The plagioclase is in minute grains and is difficult of exact determination though it seems oligoclase. Chemical composition and norm of Morris granite (15-A-3)! Pee pales oa Onin Sb: hn, | Cons By: Me | G7. RIOR el orate tea 3| © 276! (sal. «0281... .: BOA.2|| arash .633 RO) eee eeey eee unl ae Oran OA OW OONAS amd’ JOOS. ates: uexecnall cues eae BeNOR. cl Ton) 2000)... 2 Neel ners oi sere oleae ae sl YOO: pues Be Ole cs. Wnerinc| a cove cnet taco ene Were cee cael See es SOOT SOOO a oa dhe 2 MgO 0.46 OWS eevee Legere allingete arta | IAs, ea OMT Ces ct ee a CAO Seine 0.78 Ghillie SE ees Veen (OY et eee oe | Pi ceria Say, HEN aS Na.O Beed. GSA aes ise toy Ste Nts rare at De ec lal | Gg K.20 Ape 049 COV AMOH ec rato NS Picea Paacyl kak See pene te trea gest eee ele ne H20+ Oe el eee tera Pncariestiea silly sich steel tara Sool ee Lecalle andy ae at oie Wests Sh Sic, H,0— OP IRG men wires ene uae oane echancdl (ache cael isaall Sucethaue ce ee a tea Mie se mealert AMO)s OPAL eae Remar Met mem a iran iene catnatonl Nora test ses! [Ne fanro doapie! | 'esraiea ker ic ee ah areas es Pearernete ZtOz ONO? met teal hoeaes eee lh are eter lh ca ope ee beat ct| caus Vere call ent cer Bae e "Ghs OTM era een ec eee by nes dl ge eral pia Re Pear ee Leemere Seu ease OP OME ree aerate Pe, net The ercer coral eae el Nt: TAC IORI Ue a MnO... ORO Olas Soon tae |e ere Netting ae re [Peer Sar E see cy cote | pe Total OG Sills cca be 046 054 ola 008 O12 006 623 Or. 25.531 /Nieveeeee 3 a0 Class, = Eage DUSK ae 25.7 —1«z, persalane An... 13.89} 96.34 On ee Co..... 0.82 | Orden) === 225 = 0.65 = 3, columbare On) 2 37705 | P 57-77 : 4 Hy Se 2G)) Rang, Na8 Eee SS ae —— seals kaise Nee 30 | i, coe ae CaO 14 ee: 2 Subran La ue 85 = 3, alaskose Rest. 0.60 §; Na,O’ 54 3 3) Total 99.84 In the new classification of igneous rocks this granite would be called an alaskose. It is however very near the border between orders 3 and 4, so that a comparatively slight increase in feldspar at the expense of quartz would put it into the liparose division. The norm differs from the mode slightly in the quartz-feldspar percentages. A considerable portion of the magnetite of the norm belongs in the chlorite of the mode and with this would go the slight excess of alumina which appears as corundum in the norm. The hypersthene, corundum, and excess of magnetite of the norm IE. W. Morley, analyst. P2Os, BaO and Cl absent. S12 NEW YORK STATE MUSEUM would give an amount of chlorite considerably in excess of the chloritized hornblende of the mode, which has already been ac- counted for. The feldspar percentage should be correspondingly decreased. Even then the difference between the quartz feldspar ratio in the norm and mode, .65 in one case and .56 in the other, is sufficient to shift the rock into another order, .60 being the dividing ratio. The probable cause is that the ratio present in the slide is not quite normal, the quartz not being equably distributed through the rock. Syenite. The great amount of differentiation shown by the rock of the syenite bathylith has already been noted. Analyses of a considerable number of these have been already published, but there were yet lacking those of the more basic and more acid phases, and moreover the red syenites which occur in association with the granitic syenite had not been carefully investigated. The specimen of basic syenite (12-1-6) selected for investigation, was collected a little over a mile n.n.w. from Raquette falls. It is a rather evenly granular, gneissoid rock, feldspar phenocrysts being few and of small size. The thin section shows augite and hypersthene in the parallel growths which are so characteristic of this rock, hornblende, magnetite, light colored titanite, apatite, patchy, vermicular garnet, a little quartz, a little pyrite, and feld- spar which is in part microperthite and in part oligoclase-andesin. The mode of the rock, by Rosiwal’s method, is as follows: Mode of basic syenite (12-1-6) Units Units measured Sp. Gr. by weight % weight Beldspare a) eo carbines pee rae eoe 748 X% 2.64 ==. 1975 “== 5Geme OuMantas a reeicks «caer tenes ieee. eareem seas 38 X 2.65 —= tor = 2.87 Worniblenderrmemerer eee Bo O60 NO IS ea = iG) 9.65 Audgitesac. saree teeny Sinemet 2) 123 K3. 32) ==- = ACO) ee ly persthenles reat. ge ss seer ae IIL 23.35 = 37 os en MaeaWerite et smn aicie- (ec PEs coe ani AAD SSI peo) nn 6.57 Gatnet veri tthe sais ee cee nares aos a 27 0.97 7aNh DEH E Hes ena Pavan STH ee PIRI AMO Gene nbeeIb Gc WBS 2.2 == a Tash Ditanites ieee sce a eee eusmoenen ariel eae AS 35 == i = ©.40 Pye 9. Be tee aie is nee aoe ae Woe 5 = — 0.14 ‘Totalgeiciaitus cioceinuanteneen nce T194 3519 100.00 a ae GEOLOGY OF THE LONG LAKE QUADRANGLE 513 Chemical composition and norm of basic syenite (12-1-6)! Com | Mol] Or. | Ab. | An. | Di. | Hy.|Mag.| Ap. | Ti. | Qz. | Py. SiGe eee EAL LO}. 902). 190\, 300). 054).020). 107). . os (han): 002|.048 SE Ora Pea EGU OSS | OOD MOG TN loc il ndecc-si| apeeeaills'= = 2] eo spall eeolalleton ResO%..)<. 5. AENSI2 O21 etry veal auc ermied |eerseetre lenis ec 028 inl bees 002 MeO reo GEANSOOO hs. 2 ale cme lerteellle 007|.050].028 OO2 hers olece INGO ieee. EAs OsS teers Ira cuewtlies ot NXE) StS 177 Poesia lo ached [eee ey ct [cece Oe awe. (5 Le | |S 05 fo) Pere nl Ree |.076|.013 bs aeell O2elal tena ceel muses [etna 6 Wis O: 2.022. Be SHIROOU Hts eeAUOXS) | Goh 6 al\ Gees heen cee OFZ) Ow 7 FOO: a1. Miles es GOT Sa ae era aa aaa S78) sOROls Go olleooclleaoc SUC e oe allen wolice c= EMO ccce'e oa dea Lael eOvAlls ocala oe GO] aso oll-O2Tle o 50] .6Ou Nga Oar etait eee PHOS eS easel SOG Olisnatenalltatails slay scetellts m-ctelliei easel os etere 30) RAR heer ene BESO Mime OATh OAT eran rs lt own atealisaewevell at loud.llite: «Gil ates abl olen aes DO Oe 2s Sons) v a OPA cearey skewer neal onezee enter nai liste aes [tcc cma faite Mra lp caes Ilsieear BNO ic aca cia'e eee sce 0.08 (HOTEIN ded| eee Nese Le tia OOvE| Mee | to erate hotels ay oe TOOsOlo doves L04t .059 .050}.087|.043!.019|.001|. 181 Fem. 20.74 Or..... 23.02 Class, Sale caus g00' Ss 3.81 = 11, dosalane ie ie Be 6) 10. 86 Wiz). . 16.86) OE, 5 = @Scon 2 16 == 4, austrare Mt.. 4.32 Panis cKO Na20 Ree eO es ee ae Hy.. II.03| 20.74 eae 72 ee 5.22 20’ 4I : | aR A Neath) Se 55 Mies... o.17} Subrang, 1726 emo Total 99.64 The rock is close to the division line between orders 4 and 5, so that it is a harzose very close to shoshonose. The slides of the type syenite from Loon lake, analysis 5, have been mislaid and could not be found, so that the readjustment of the iron percentages had to be based wholly on separation of magne- tite from a weighed amount of crushed rock by heavy solutions and magnet. The result gave 1.58% of magnetite, or 1.090% of Fe,Os, which is certainly much more nearly correct than the .42% of the original analysis. Its norm would thus become: 518 NEW YORK STATE MUSEUM Or. cee 30.41) Sal 92-42 rao Gare aia see Class, neane Baa TE 6 5 1, persalane BN ca gee aes Order Oise ee a 07 = 5, canadare oasce O08; Ape Se eae Any (9) Mt.... 1.58} Rang, oes Nee, pega = 2.6 = 2, pulaskase Ding ei. a 7.94 Bae 52 IBD¥oone Aall® é 20’ 5 : i Sieben 0.17] Subrang, NEMO oe .68 = 3, pulaskose Total 99.36 The rock falls close to the boundary between subrangs 3 and 4, or is close to laurvikose, showing thus its close relationship with the considerably more basic rock of analysis 3. The Little Falls rock (analysis 7) has beautiful cataclastic structure with the production of much finely granular feldspar and quartz which can not with certainty be distinguished in the thin section. The quartz and feldspar had therefore to be measured together in the determination of the mode. Mode of Little Falls syenite (toscanose) analysis 7 Units Units measured Sp. Gr. by weight % weight @Ouanezrandteldspar ee eee ee ) PSEA A,Or == 7A == 87 2s MonmMlplemcle neers neat etene eieaeasione ene WWOKA.4 = Col = 7.08 yO XM Se 0. Marcia a ek tonteeper eee eee FOR G39 == 16: = T.94 Mralem ebite allo: rater ooneh ni caey cay oa inet eee BO eis 25. oe TS BIOTIC Es ics eater tetra. Roney ae 20% 3) = oo 0.40 ADAGE: ORME snes d Cita tae weerahe Bre etee) ceapectoite I3.2 = 20) == Osu dl Diteeshat Cranes MI erate, ye tua Recetas E25 = 25° = 0.44 DAL COM os ini aratee ws aemeieicne meee iate REL == ma = 0-14 DY TICE Rass aca hs Oe eee ees BS a ri == o.18 MO tial cessrve se axctewacocet ate gate ster ete ace 3168 8529 99.98 Norm of Little Falls syenite Oreo eessaaell C Sal oe 5a sa 1 Ab.... 36-84) oy 5; ea 8.04. 0) = eee An.. 7.78 : PEO AE 13 Arjen he , ; Oz Le UB ae? | Order, icersaon ae 17 = 4, britannare Mt. 1.85 | Rang, Ott Nave ES 6—= 2, toscanase IDK. 223) 69) out ee EE ae Le 3-59 Subrang, B20’ __ 547 fe Ap 6:37 >. Nas Saab ae .67 = 3, toscanose Total 99.55 The quartz-feldspat ratio is nearly low enough to throw the rock into order 5 instead of 4, so that it is a toscanose close to pulaskose. GEOLOGY OF THE LONG LAKE QUADRANGLE f 519 The mode of the rock of analysis 8 showed 1.86% of Fe,0,, and the original analysis was corrected on this basis, so far as the iron values are concerned. The norm, and position of the rock in the new classification are as follows: Norm of pvroxenic hornblende-toscanose (analysis 8) PicWadt SAS Ce aE Pee lien Onr | Abe | Am (DE eye | Mt. |) Ap |t@z, SQ) sa eee asec Oe eH Hs AAS 27/6) 49) OSl| OAS] roles E|4 een olla owe & 5 Bi AllbOs ocoacésode0 2) Td SOON. co MAA OOF -OSOM OG eu solace claeccicces COs |e nes | ellen a eas E SIS eae WIROR Ole seme ccc ralhsher walls ccccilirs sacl a6 © illow oho) ate 2 Gece Motales <3. Tae | eeeeene .058 pba ere .028].048 .018].001].001|.143 SSS Or. + 32.47 Class Sal: a Bon87 = 6.47 —=11, dosalane Ab. 34-581 96 87 Setar 13.43 3 = ae Order Os SEO es TI = 5, germanare Oz... 8.62) R 78.25 : 5) Bie. 3-29] K;0’ + Na.O’ 124 Hly-... 5.42| Rang, ; = == 2.1 == 2, monzonase Mt. 4.29} 13-43 ae ge BP eee ee Subrang, NEOe = a = .9 = 3, monzonose fs On the border between classes I and II, hence close Total 100.30 to pulaskose. A comparison of the two analyses shows a reasonably close agree- ment in all respects, and indicates that microscopic analysis fur- nishes a means of quite accurate determination of the composition of these rocks. It shows that the feldspars have closely the as- sumed composition, and that the hornblende is probably tower in ~ silica and higher in iron than the Californian hornblende used in the calculation. The norm calculated from the result of the micro- scopic analysis would closely agree with the other, and serve equally for classifying the rock. A comparison of the analysis with those of the green syenites shows a close agreement, the main differences being the different ratio between the iron oxids and the lower magnesia of the green I Sp. Gr. 2.735 at 18°. E. W. Morley, analyst. 522 : NEW YORK STATE MUSEUM rocks. The field evidence of close relationship between the rocks thus receives forcible corroboration. One half mile east of the locality from which he previous rock was obtained, on the north line of Litchfield park, occurs a beautiful, coarse red syenite which differs from the last in holding little or no quartz. Its calculation follows: Mode of red syenite (monzonose) 10-C-1 Units Units measured Sp. Gr. by weight % weight Micropentiite ). sir ome ate elev aire) 1463 %2.60-- == 380305 Plagioclases a-ee rei onerciee rierr ‘296% 2.63 — 786 = 13.58 Hornblende. ........22.+-+ssseeee 267 X%3.2 0 == 854 ire Otiartzaey-neort-ner IPS Sa eA Ne De 62x%2.65 == 164 == 2.84 NBII cn shod soo auc soesecdea 22K 5.25 == 168 > — 2.90 ANON 600004 Pu asta vate Reade oy sc Mee ouetishahs IX3.2 = = ©.05 BUREN, 9 Sb 5.0 690 Gee ee ersn Svar egeues tates: 2X4.3 == > = 0.15 ANoneUleeeah SEO Hao fOr. 6 auc co 2126 5787 I00.00 Composition and norm calculated from mode a Oy, || Orel, Alb. Anor. | Horn. Mag. Apat. Zire. Total toh O) enencke eee Pee) eles Bole | PU RCOKS)|| Me oly, Vf e2O)|o os wa Alo aS 0.05 61.02 INlAD a aie soe ale 624). 906!" 93.33) nO Sls ses oer ie ey ysl IRS Oe Hel ome all oe ibis een nico oA © 7'5| =.2 7 OOll.. tcc a | eee 2.75 ACO) urea Parag baer en Al Cen Nn eC) OsOGlscascoilocooc- 2.54 IMGHO)S 5 o don 3 Baedy | ele etn eae ATENEO is oot (tue ay cS 2 OTe cv Altar eae Ree ere 2.01 CaOnee ees: Prensa stoes allies feces ake Abuemsts el beae fates ROMs mig o 6.4 3.68 Nae One acas ifs | Ome ea A210 || meee @oeditle She. 2 sth eesneceee oes 4.4¢c OI Ols Mere Sees lahis kc 2 eeorene i eres ESOS ri eneErS olooc cos So 77 PAO Reis ts 50 eae ae a earns tale eka ol ara tell no Hig oe QAO oo cce @) 502 LOR eee RS ae heals tree Sul ieenonataee ueoin ae autoNG cocks oso ¢ ©. FO| a On HO Total. .|2.84| 33.99) 36.25] 9.06) 14.76) 2-90) 0.05] 0.15 100.06 The calculated norm is: Or. Ab. An. Dit ey ete Ozoe Bid 5 Bi 20 II.40 5. 83 AGA SO Oh ey eae Class, pal — S55 = 6.0 — 11, dosalane Fem. 14.26 QO 2.82 Order, Tvs ean yeaa .034 == 5, germanare R ng. K20! + Na2O' __ 132 2, monzonase a | ee CaO’ 7 66s See a : K20' 61 S Spee jae ait ubrang, NELO? GeGe . 86 3, monzonose- Judging by the previous case the silica and iron are a trifle out of the way, the former too high and the latter too low. It might be legitimate to modify the analysis proportionately with the differ- ” e GEOLOGY OF THE LONG LAKE QUADRANGLE 523 ences shown in the two analyses of the previous rock, but these would affect it but slightly, and since the trouble with the previous analysis may be mainly owing to the fact that the normal amount of magnetite did not get into the slide, rather than because of dif- ference in the composition of the hornblende, the change might not be an improvement. The analysis is confidently regarded as an accurate expression of the composition of the rock, which is some- what more basic than the previous one. As a sample of the more granitic syenite of this group a rock was selected which outcrops on the road from the Litchfield gate to the boathouse on Tupper lake. It is quite similar to the rock of which the lodge and gate are built and it outcrops over a wide area within the park where it seems to shade into the green syenite. While some portions of the mass may be even ‘more acid than this is, none is greatly more so. Mode of red, granitic syenite (toscanose), 869 Units Units measured Sp. Gr. by weight % weight Miferomertinite: . cc Uk ca. costes as as 1907 X2.6 == 4958 == 67.20 BPP IMOCIASC sn ces Portresisacc can was os 2ST 22.63 = %72OQ = 1.0% PRB Merc acN S GS ace baie snane’Soace ASRE 2 OF == 1rd s= nO, pA —. SSICICIIETRIG KSA Ne trae eae emer ee IO7 BQO = 23 = 4.63 SPENT bILCHace tn ats eicpartene bese. 1s Gosia Stora ete DiS OS == Tio == T.40 2 LISI Bee RSE oe hae 2a On —— —— O.12 A DRL Ee SU game ere cha cea OxX2.3 = i = 0.25 MP MIGEO [ieee ics Mtoe See asd ae See deen afed PeA.5 4 = 0.05 “TNGTE AOA es co Cea re en aos 2778 7379 99.99 Qz. | Orth. | Alb. | Anor. | Horn. Biot. | Mag.| Apat. | Zir. | Total BOs ss. 1G. PA DE pA OG Ball DEOol “OcORleE 6 clloomoak 0.02) 68.15 OS ae Gia OOO Nees OMA A MO.4O2| ee ills atone eral scares 16..53 Bane) ete rare mn Meee oe cca Poca a Syne ome C2 S| SEO OTT, «O12 Mire ene ote |Iot ets 1.26 UO eran al sac nstadell alto S| oel te a igts a os: » Dahil QrOZ Owes cacaleace I.00 EPR fre |= ais ell oats, soto as shel ane wiere Chale} SOMO ale eee || Poececeate ko cack 0.64 MOO) Preset civ Sic ctlouiek axe slic stevens Th5 el Ons illeomneee 4 o|| -2@aars 2.48 1S iO) ME ese He ae AMES lew eis 2 OR Ori heerssa aS En yal tty 4.22 2 OT eceanie| eee ee GO herausie ld acca s GeO2miOF OS encnhlic ee ens 5-59 Bera Ores nets 8 ate cara ieee lh emer ltewcnevecsololer saa esd ae eo a8 a 0.10 0.10 © cere Ga eget: ae eos kets 22a Ie ees ee ee | 0.02 0.02 = FO Ss GS tedSihes cell See lee ee ee | sare lee ee O23 ORs Total LO@24133 200/35 .30) S285) 4.63] ©.12/T-49|, ©o.25|0.05|/100.02 524 NEW YORK STATE MUSEUM v From which the norm is: Ors Ab. An. Mt. Di. Hy.” Qz. Total 33.08 35-32 9-79 iota) 1.40 16.36 99.82 Class, 26): = Dasa) ele persalane Fem. 5 oA CUS OsSO as ae : Order, Fa en — .21 —4, britannare Ran pea Neos 2.9 = 2, toscanase ang, Cad’ ra 30) == 2, CS K.O’ alee 5@) ‘hs Subrang, Neo or .88 = 3, toscanose A coarse, red, porphyritic syenite which is very quartzose, com- poses the steep cliffs on the south end of the big ridge known locally — as Follensby mountain, which lies southwest of Follensby pond. Its mineralogy is the same as the previous rocks except for holding augite in addition to hornblende. In the calculation the augite was assumed to have the composition of the diopside from the laurvikite near Laurvik, Norway.t While that is more basic it is otherwise a similar rock to this, and the augite has the same char- acter as that in the more basic syenites which closely correspond to Brogger’s rock. For the sake of brevity the details of the calcula- tion are omitted. Mode, composition and norm of toscanose (10-D-3) ee Units measured % weight Composition Norm Microperthite 1760 59.50 | SiOz ya ay, | OT eter 26.80 OMe s se sin sos 898 20.03 | AlzQ2--.>- 13.39 Aloha es arene 28.98 Dlacioclasear ar: qa} 2.47.| Fe2O3....- O9AG0 | UMilsss socscs 7.48 Hornblende..... ON ve wait INOS es « Oh Wig |= one yee Ber /NbkeaNK Sc ao bdo 6, 1 2.87 | MgO...-.- 6.81 | diy. oo. eee Magnetite......- I OnO7 | CaAOle tr 2'.374, |. Mites aoe 0.37 Apatite........- I onode |) NaZsOheacr 2-43. |wOz: ee eee 31.04 ; KIO ren 4.53 IPAOeae dob 0.02 Mi@tale a sckerere = 2895| 100.00 99.63 100.22 Sal. 95-90 i ie : Class F eee as 19 = 1, persalane Op isn BL Sea cre Order, SaEG 18 4, britannare Rang 0" 7 Naz0 193 9 4 = 2, toscanase » CaO’ CE ee K.2O0’ 48 Subrang, Naso) Sens .87 = 3, toscanose —= = oe ’ 4 1 Brogger, Eruptivgest. Kristianageb. 3:23. GEOLOGY OF THE LONG LAKE QUADRANGLE 525 This is the most acid of any rock yet analyzed occurring as a part of the general syenite mass and is an unquestionable granite. It is quite close to order 3, and though not quite so acid much resembles the Morris granite in composition, except for the higher lime. For convenience in comparison the four analyses, and that of the Morris granite are here placed side by side. ————————————| I II Til IV Vv 23 GOR NS ee ce ae 61.02 62.85 68.15 Fakg BG) 76.41 lg ee a ele a Ip Gp 16.80 16.53 13.30 TeaieAar MeO etcl ele Saisie: 27.5 2.96 1.26 0.26 I.O1 Me alate ees 2.54 2.89 I.00 Oni 0.50 RD) GRe nee RE Oe oan oe taal 2.01 r.48 0.64 0.81 ©.46 2 oy Rae ee nae an 3.68 3.24 2.48 2.34 0.78 Oe ne Lee er 4.40 4.09 4.22 3-43 3.34 25 Ee eee any] 5-49 5.59 Agia 4.33 5) SE 2 SURES pee a ao al as (OW AIZGl veh Pear asta |e se eae 0.34 | O=, 5 Se Oat OiHT 3g lie anor | eee S 6), 18 Ba yer eee ek OOO rel arre ee pe ek st 0.03 DS od at a aaa 0.02 0.13 0.10 0.02 trace "soo ie BRL ae Stearate he eae ene Ian 0.01 CNA gl Wee Aart 0.01 RM sits ores ess se cl pe re ONO 2a nana ale ete ©.O1 OS 0 eee ane a oe aa 0.10 trace QROBs Peters, 0.02 AS ee eee ee eel Opn nse a Saale opt 0.06 BO... a lhig Sole 08 Seagal pee ORO mM Maite s ake eellt tos Ge trace otal. Coe sh ot ickes 100.00 | 100.69 | I00.02 99.63 99.84 eee eee I Syenite, (monzonose) 10-C-1, microscopic analysis. II Syenite, (monzonose) 10-B-2, E. W. Morley, analyst. III Quartz syenite (toscanose) 869, microscopic analysis. IV Granite (toscanose) 1o-D-3, microscopic analysis. V Morris granite (alaskose) 15-A-3, E. W. Morley, analyst. Grenville igneous rocks. There occurs in frequent association with the Grenville sediments of the quadrangle, especially with the quartz gneisses, a rock which is not especially gneissoid, has an igneous look, and also at times appears to show igneous contacts against the quartz schists, though these are so disturbed that it is difficult to be certain in the matter. The texture is fine grained granitic, with abundant glittering feldspar cleavages, and the color is a grayish white, with a smack of a flesh-colored inhoere. We ahs fairly easy rock to recognize, though difficult to describe with ex- actness. If an igneous rock it is certainly of much greater an- tiquity than the big intrusions, and to class it with the Grenville, with which alone it occurs, seems the obvious course. Its chemical composition is as follows: 526 NEW YORK STATE MUSEUM Composition and norm of Grenville quartz-syenite (dellenose) 1-M-5 from near Lake Catlin comp. | ratio, | OF | Ab. | An. | Di. | Wo.! Me. | i | ysl) SIOZ ae ee 68.66) .144 |.479|.199].028].041|.009]....|.002]....|.386 ae Mapalen ee eee oy Sole Aelbe AS gon all avo! Bere Co Oa ieanie DE OO| sO oa ene eeahen Raley els oial|s cco s PCO ss eeieere IRAP aa Oiss= |peewwraltecucallaS oe 17! I INGO ce reese cies Ory ACen Cole || eters craeel eraser 10) (Peers PRE tro Gil'5.c Gc|lc o = os ea keg tear 2.63) 1047 r4| 21 9 Py Pete cet BO me ae Mee 205) LO 3a Nhe call = BSlle Ge alecs flisesc ce | cee meg eee 1G O tease he Sosa 7.50] .080 XS ha-shaual| oo Seo waited) sos keadl x Jere) Sil gee | Fs @P pent. Sane Ol beted tee eae alll Shane Meee OSIM erick Sileicsclla sc - Jal @ ay reste ec (oo C10) (aries rere aioe eisai Meee lees cially ss ol1o cclsloe « - AOD see ores etek Sig HO)! doally seers. | OG) OG ncsae .080] .033].0T4|/.041|.009].018].002]....|.386 | Or..... 44-37) Class, Sle 5 8.5 = 1, persalane IND)o 9 a0 ee 88 86 HEM. ~ TO. ZO S on che i a Order, 2 = a .35 = 4, britannare Des Sag. ahaO | | : ACY Woks: Ago Rang, ED Wa 2 Gis BE) es .4 = 2, toscanase AS a 4-20! 16 39 eos : Aq Seed age O-33 Subrang, = =: a 2, dellenose Ihe oo | Oe 8 >’? Na,O 33 NOs goa Oct Total 99.25 E. W. Morley, analyst. Chemically this rock is sharply distinguished from the syenites by the somewhat lower alumina and soda, and the high potash. The slide shows the feldspar to be mainly microcline, though with some microcline-microperthite and microperthite. It shows con- siderable quartz though by no means so much as the analysis indi- cates, and the dark colored minerals are augite and titanite, very little magnetite being present. The augite must therefore be high in iron. The character of the feldspar is quite different from that of the syenites, as indeed might be expected from the analysis, and this constitutes the main difference between this rock and the syenites. The augite must alsg be of quite different composition. GEOLOGY OF THE LONG LAKE QUADRANGLE 527 The analysis seems to warrant the conclusion that the rock is an igneous one, and if that be true the obvious differences between it and the eruptives previously described suggest a separation from them and likely an age difference. Pyroxenic amphibolites, hornblende-andesin tocks with acces- sory augite, hypersthene and magnetite, occur in abundance asso- ciated with the distinctive Grenville rocks and have been described by all workers in districts where these rocks occur. They have been sometimes regarded as sediments, and sometimes as igneous rocks. The appended analysis is therefore of interest. It is the average of the three best analyses turned in by a class in quantitative analysis, and is therefore not of high grade. In con- sideration of the close supervision however, the close agreement between the three, and the general high character of the work done by the three men, it is thought to be worthy of respect, in con- sideration of the lack of better analyses. The rock was a Grenville amphibolite occurring south of Follensby pond and not far north of Moose creek. ee en ee ie ee CR 7at See ee ee ene Ot ee ee 18-75 re ee ee eel le Sete Th cites ee ete Ree oe Re Bhatt ee ere 9.78 er re IE en 4.86 Jocks +o oelagts a RiSsBIc lacy Sieg tm alle eg ia nme ea 2.42 Lr IS d ekle.o 8 AaIRtr aia Rm fen Sa ene ato oy gd bd sland Rte cM Ian ater te Raia ett a e. er ee ee 0.25 SHOUEI 2 0 5’b.0 tik cutke omental eet ea a 99.59 This is the composition of a diorite, or gabbro, and suggests, though it does not demonstrate, the igneous nature of the rock. If it be igneous it likewise is probably a much more ancient rock than the gabbros of the intrusions, INDEX Acknowledgments, 41. Adirondack forest, disappearing, 453. Adirondack rocks, early Precambric age, 453. Alaskose, 511. Allanite in syenite, 516. Amphibolite, in anorthosite, 476; in Long Lake gneiss, 465. Amphibolites, 464; pyroxenic, 527. Amphibolitic gneisses, 464. Andesin in Grampus gneiss, 468. Anorthosites, 455; Whiteface type, 468; description, 470-76; gabbro . border, 473-74; outliers, 474-76; syenite younger than, 479; as building stone, 502. Apatite, in anorthosite, 475; in Grampus gneiss, 468; in Grenville rocks, 508, 300; in syenite, 512, 516, 518, 520, 522, 523, 524. Augite, in anorthosite, 471, 475; in Grenville rocks, 526, 527; in syenite, 512, 515, 516, 524. Batholites, 454. Big Simons pond, 452. Big Tupper lake, 452. Biotite, in Grampus gneiss, 468: in Long Lake gneiss, 464; in syenite, 516, 518, 523. Bronzite, in syenite, 516, Building stone, 502-3. Catlin lake, 452, Chalcopyrite, in anorthosite, 471, 475. Chlorite in granite, sro, 5It. Cold river belt, 450. Corundum in granite, srt. Dana, J. D., cited, 507. Diabase, 484. Dikes, 456. Diopside in Grenville rocks, 461. Drainage lines, 493-05. Drainage modifications, 499-502. 529 od Economic geology, 502-3. Faults, 457, 488-00. Feldspar, in anorthosite, 471, 475, 476; in border gabbro, 474; in diabase, 484; in Grampus gneiss, 468; in granite, 482, 510, 511; in Grenville rocks, 461, 504, 505, 507, 508, 509, 510, 526; in Long Lake gneiss, 464 ; in syenite, 477, 478, 512, 516, 518, 520, 521, 522, 523, 524. Foliation, 484-85. Follensby pond, 452. Gabbro border of the anorthosite, 47374. Gabbros, 455, 465, 466; description, 483-84. Garnet, in anorthosite, Aili, AD? sain gabbro, 483; in border gabbro, 474; in syenite, 477, 478, ASOD Inia), Airis, 510. Garnetiferous gneisses, 462. Geology of Long Lake quadrangle, 453-59. Glacial deposits, 495-97. Glacial erosion, topography modified by, 498-99. Glaciation, 495-502. Gneisses, of igneous origin, 454; doubtful, 455, 463 ; quartz, 460; sedi- mentary, 461; as building stone, 502. Grampus gneiss, 463, 467-60. Granites, 455, 478; description, 482- 83; dikes cutting anorthosite, 475; as building stone, 502; petrography, 510-12; analysis, 525. Granitic gneiss, 467, 460. Granitic syenite, 478. Graphite in Grenville rocks, 461, 502, 506, 508. Grenville series, description, 454, 450; associated rocks, 462: uniformity of structure, 462: lie in downfaulted troughs, 490; petrography, 504, 525. 530 Hobbs, W. H., cited, 493. Hornblende, in anorthosite, 471; in border gabbro, 474; in Grampus gneiss, 468; in granite, 482, 510, 511; in Grenville rocks, 461; in Long Lake gneiss, 464, 465; in syenite, 477, 512, 515, 516, 518, 520, ali, aay Salas yl. Hornblende-andesin rocks, 527. Hyperite, 465. Hypersthene, in anorthosite, 471; in granite, 531; in Grenville rocks, 527; in syenite, 512. Igneous intrusions, 455. Igneous rocks, 454; later, 456; petrog- raphy, 510-27. Jenkins pond, 452. Joints, 485-88. Kemp, J. T., cited, 460, 468, 474, 480, 465, 502, 503. Labradorite, in Grampus gneiss, 468. Lake Sanford, titaniferous ores, 502. Lakes, number in Long Lake quad- rangle, 452; in St Regis quadrangle, 407. Little Falls syenite, 518. Long Lake gneiss, 463-67. Long Lake quadrangle, situation and character, 451-53; general geology, 453-59. Magnetite, in anorthosite, 471, 475; in border gabbro, 474; in Grampus gneiss, 468; in granite, 510, 511; in Grenville rocks, 509, 526, 527; in syenite, 477, 512, 513, 515, 516, 518, 520, 522, 523, 524. Meade, A. P. jr, acknowledgments to, 451. Mica, in Grenville rocks, 461, 504, 508; in Long Lake gneiss, 464, 465. Microperthite, in granite, 510; in syenite, 477, 515, 516, 520, 522, 523, 524. Monzonite, 477. Moose creek belt, 459. 5 NEW YORK STATE MUSEUM Moraines, 496. , Morley, E. W., cited, 505. Morris granite, 482; analysis, 525; petrography, 510. Ogilvie, I. H., cited, 467, 491, 495. Ophicalcite, in Grenville rocks, 46r. Paleozoic submergence, 456-57. Pegmatite of Piercefield gneiss, 460. Peneplains, 491-02. Petrography of the rocks, 503-27. Phlogopite mica, in Grenville rocks, 461, 504, 507, 508. Pickerel pond, 452. Pickwacket pond, 452. Piercefield gneiss, 463, 469-70. Pitted plains, 497-08. Precambric rocks, four great groups, 453- Pyrite, in syenite, 512, 513, 516, 518. Pyroxene, analysis, 504; im border gabbro, 474; 468; in Grenville rocks, 461, 504, 505, 506, 508, 509, 510; in Long Lake gneiss, 465; in Piercefield gneiss, 470; in syenite, 477, 518, 520. Quartz, in granite, He 482, 510; in Grampus gneiss, — Grampus gneiss, 468; in Grenville — rocks, 504, 505, 506, 507, 508, 500, — 526; in Long Lake gneiss, 464; in syenite, 477, 478, 512, 515, 516, 518, 520, 522, 523, 524. Quartz gneisses, 460. Quartz-pyroxene gneiss, composition, 506. Quartz syenite, 525. chemical Raquette river, 452, 490. Road metal, 503. Rock pond belt, 450. Rock structures, 484-90. St Regis quadrangle, number of lakes, 497. Santanoni quadrangle, 474, 402. Saussurite in anorthosite, 472, 475. Scapolite in anorthosite, 476. Seward pond, 452. INDEX TO GEOLOGY OF THE LONG LAKE QUADRANGLE Shonkinite, 477. Smyth, C. H. jr, cited, 479, 503. Striae, 495. Syenite gneiss, 460. Syenites, 455, 473; asymmetry of the syenite differentiation, 478-79; basic, 478; as building stone, 502; descrip- tion, 476; granitic, 478; green, 515; normal, 477-78; petrography, 512; red, 475, 519-25; as road metal, 503; younger than anorthosite, 470. Titaniferous iron ore, 471, 474, 502. Titanite, in Grampus gneiss, 468; in granite, 510; in Grenville rocks, 461, 504, 505, 508, 509, 526; in Piercefield gneiss, 470; in syenite, 512, 516, 518. Diora Topography, 490-95; as conditioned by the rocks, 492-93; as modified by glacial erosion, 498-09. Tupper Lake reservoir, 452. Tupper syenite, 476, 470, 515, 510. Valley plains, 497-08. Whiteface type of anorthosite, 468. Whitman, J. M. jr, acknowledgments to, 451. Wilson, H. M., acknowledgments to, 451. Zircon, in syenite, 516, 518, 520, 522, 523; in Grampus gneiss, 468; in granite, 510; in Grenville rocks, 504, 505, 507, 508, 509. ~ Oo Sa dale a day Sk” oF OE oN rm ROL i oo 0 a Se Fee ie a, ey Ret ll LTE OY mem ee O47 OA fori WN RO O84 ise SSN See I re ee 11 rie ee NSE ee Cli ose — PRM iis eS ASS; NS Oy fit ome PARANA A eS NR PN LS fees Hy ANA RR AURR Ladson ae NSSSR SS) (SEAN A citer oe bout SRR ss TAPS SSSR RNG 1 GR ee SAN HEELS SEAS i PB a ee ES OSA ie SSS? GANAS er AN HE = SSS Sao Wy ater BRR RAITT HV We ca SSRN Nita gets {hn SSS NS. OEP LPE EEL Ae nn, eet an A NO > SSE VUE TEP TES ad RAN Sa TA GL NANG Bn WS ON QOS ZAS SEN RSE ARREST QRS Ze DIN pm BONN SSS SN NVI Neaeeees epi ify SSI AVN WR RB See AA eee = eS NERO}; OS < FO) I re elie en OS) KE Le hoy paral eee NN ots © WN a ee) en RI NS SS ipree Winess, Geeecs 2 SNe eee ALN Wee ry \ iy FZ ~ Y ZEW) OGLE \\\" i OG, 8 > WW 6 QF 4 BEF Sam WEAR RIOS rh NSA} VG oe OEE AWWA RAD} CEE ede Os Yar. SLE eA ROSS Tey ERS Faro. PENRO NTE, A lind PA BANNAN ANA een TOI YY 9 PANN TALS TT MIA So AVR SS? FMT Ne Hi, at A GEEZ ZINN AWN i SSS)! SA OILII) SW al) MA a ) bY 1/411 me LF NA OST) TE MAIN NL OG EEN Tas WO TS a) HGR Sg 2a Vib ss Tay = LESAN SS | > ye Ei = bet Ja beetle) 4 Ny LINN WV Nie IW WN = aws i = \\\\ Whee > Sa Wh LS ee NIT STP Ns 0 Fe SRS NUL 2 HHH ES NS AWB MAH HH) ies Sew iis NTT LRA GME LSS SS CMG SSS PT © ES oat SS SSS SSS Aen = DVO fb 5 a ee LO SE SSPOLS SO erry ried Vimeo 4 - Ce Ha NY 4 DIN e SS Se) SP A SNS 6 Oey ER ORS NZ ATR Ye HONS Se )))\))) ANY ThE GRR So i rreees “poe al Ae RAGS HN Ne) ian oo a Hh RH > i eee ee, HAWN Ae eae Lh RRERE BHD Wi "AZZ eos)” OI Ce os Ae NN ME CM\\E acy 2S ate | RANE OAR AYU CofE OSS SSAA UD ey MAS Ss Se eS a RUT BR NS Ss Fe IID ® = OS Se eT LD) py pis, NT SZ FAW (aa —— Age eS SS OS eS > WA ea = Saya lwant)4=— = CE) BY ae SSS) es ——— N\A A Ne ame BIO aor, an ( PC is 6) min an H Mo Nope NK \) heme CS ene THHE Nee at ee Uw Nec fe 1 NS riaclal SULLA + Actual limestone outcrops seen EDUCATION DEPARTMENT JOHN M. CLARKE UNIVERSITY OF THE STATE OF NEW YORK STATE GEOLOGIST STATE MUSEUM BULLETIN 115 LONG LAKE QUADRANGLE Topography by U. S. Geological Survey In Cooperation with tho State of Geology by H. P Cushing Serle sabd0 1902-1904 ue New York. 1901-1902 4 5 F 3 3 A 5 Kilometers ps va Contour interval 20 feet APPROXIMATE MEAN Daturn ts mean sea level. NECUIMATION SE cealing underlying for- mations Sands deposited from glacial streams Igneous rocks i-—=2, Diabase dikes Gabbri ally with amphibolite border Red Morris granite Red to green quartz- ose syenite, forming a granitic phase— Simons syenite Green y syenite usually augite syenite; mostly very feldspathic Tupper syentre Basic border phase of LATE SERIES EARLY SERIES syenite, and grading into it Anorthosite, with some patches of anorthosite- gabbro Gabbrole border of anor- thosite, which grades into it Doubtful rocks Red, gray and black gneisses, mostly igneous and of granitic, syenitic or gabbroic composition, and of uncertain age Sedimentary rocks Grenyille series Crystalline limestones, quartz gneisses, graph- itic aud garnoetiferous gneisses, mingled with igneous gneisses Strike and dip of foliation Glacial strine ats Actual limestone outcrops seen PRECAMBRIC ROCKS PLEISTOCENE ROCKS IM TRAS 3a spiny ‘ ‘ : —! S ar Ser ety Sap ath LR TER CPonaeyAe CGR ROP 4 Sees at A, a) Page Ra IAL ora el oa : , aia nie rir comm nish iy A Pi ‘ Q 0 i Sahel } ew York State Museum ‘Joun M. Crarke, Director Ca Peck, State Botanist Bulletin 116 BOTANY 10 * PAGE | - Q Brrciion ...7....2..t<..,#«04 5, 1, Remarks and observations.7-.. 2% es added to the herbarium... 9 | Edible fungi.....2............5 butors and their contribu- © | New York species of Hyg rophorus ee Pivoecattotes. fate tOs lg Nev York species of SISSE Ds soe \ot before reported....... 17 Explanation of plates ...........- 99 bod PUGS see ocx ook ee cael ed arte EE Pa 4 , 7 2 7 Z * * , ALBANY , YORK STATE. EDUCATION DEPARTMENT STATE OF NEW YORK re EDUCATION DEPARTMENT _ Regents of the University if Se With years when terms expire 1913 WHITELAW -Reip M.A. LL.D. Chancellor . New York 1917 St Craig McKetway-M.A. L.H.D. LL.D. D.C.L. Vice Chancellor Brooklyn 1908 DanteEL Beacu Ph.D. LL.D. : : ; Watkins © 1914 Puiny T. Sexton LL.B. LL.D. a Palmyra to12 T. GuitForp Smite M.A. C.E. LL.D. eS Buffalo 1918 Wittiam Norrincuam M.A. Ph.D. LL.D. Syracuge I9t0 CHariLes A. GARDINER Ph.D. L.H.D: LL.D. DiC ds, : : : irk : New York 1915 ALBERT VANDER VEER M.D. M.A. Ph.D. LL.D. Albany Igtr Epwarp LauterBacH M.A. LL.D. . 4 New York 1909 Evcene A. Pawpin LL.B. LL.D. : New York ‘1916 Luctan L. Saeppen LL.B. Plattsburg : Commissioner of Education : 4 »AnDREW S’ DRAPER LL.B: LL Dp, Assistant Commissioners : Howarp J. Rocers M.A. LL.D. First Assistant a Epwarp J. Goopwin Lit.D. L.H.D. Second Assistant q Avueustus S. Downine M.A, Pd.D. LL.D. Third Assistant™ Secretary to the Commissioner Hartan H. Horner B.A. is d Director of State Library Epwin H. Anperson M.A. 4 Director of Science and State Museum a Joun M. CrarKe Ph.D. LL.D. _ Chiefs of Divisions Accounts, WiLLIAM Mason Attendance, James D. SULLIVAN : Educational Extension, WitLtiam R. EastmAn M.A. M.L.S Examinations, CHARLES F, WnHEELocK B.S. LL.D. Inspections, FRANK H. Woop M.A. Law, THomas E. Finecan M.A, School Libraries, Cuartes E. Fircu L.H.D. Statistics, H1rAM C. Case Visual Instruction, DeLaycry M. Eis New York State Education Department Science Division, January 18, 1907 Hon. Andrew S. Draper LL.D. Commissioner of Education Sir: I communicate herewith, for publication as a bulletin of the State Museum, the annual report of the State Botanist for the fiscal year ending September 30, 1906. Very respectfully Joun M. CLARKE . Director State of New York Education Department COMMISSIONER'S ROOM Approved for publication this Sth day of Janwary 1907 Ad iofet Commissioner of Education New York State Education Department ~ New York State Museum Joun M. CLarkeE, Director CuHaArLes H. Peck, State Botanist Bulletin 116 BOTANY 10 REPORT OF THE STATE BOTANIST 1906 Dr John M. Clarke, Director of Science Division: I have the honor of submitting to you the following report of work done in the botanical department of the State Museum during the year 1906. Specimens of plants for the State herbarium have been collected in the counties of Albany, Columbia, Dutchess, Essex, Fulton, Greene, Hamilton, Herkimer, Madison, Oneida, Putnam, Rens- selaer, Saratoga, Steuben, Suffolk and Warren. Specimens of New York species have been received from con- tributors and correspondents, that were collected in the counties of Albany, Allegany, Chautauqua, Columbia, Essex, Fulton, Herkimer, Dutchess, Madison, Monroe, Oneida, Onondaga, Orange, Orleans, Rensselaer, Richmond, Saratoga, Steuben, Suffolk, Tompkins, War- ren and Washington. The number of species of which specimens have been added to the State herbarium is 156. Of these, 60 are species new to the herbarium, 96 are not new. Of the former number, 20 are con- | sidered new or undescribed species and descriptions of these will be found in another part of this report. A list of the names of added species is given under the title “ Species added to the herba- rium.” The number of those who have contributed specimens is OT. This includes many who have sent extralimital specimens or speci- mens simply for identification, but if the specimens were in good condition when received and were suitable or desirable for the herbarium they have been preserved and credited to the sender as a contribution. A list of the names of the contributors and their respective contributions will be found under the title “ Contributors and their contributions.” The number of species found or of which specimens have been 6 NEW YORK STATE MUSEUM contributed that are deemed new to our New York flora is O7aee record of these with their localities and descriptions of new species is given under the title “Species not before reported.” Descriptions of five new but extralimital species and one new variety have been added to this chapter. A record of new stations of rare plants, of new varieties and forms of well known species, remarks concerning distinguishing characters of closely related species or observations of unusual features in some species are given under the title “ Remarks and observations.” The number of New York species noticed in this chapter is 27. ’ The study of our fleshy fungi and the collection of specimens of them for the herbarium have been continued, though much of the — season has been singularly unfavorable to their production. Rain — and showers were frequent in the early part of summer but the prevailing low temperature was detrimental to the growth of these plants. As the weather became warmer the rains ceased and ex- cessive dryness prevented their growth. September is usually one — of the best months of the year for mushroom growths, but this — season it was one of the poorest. Late fall rains, however, brought out a delayed crop which was available at a much later date than usual and helped to make good the deficiency of the earlier part of the season. The number of species of fungi added to the herbarium is 39 of which 17 are new species. The trial of the edible qualities of our wild mushrooms has re- sulted in adding I1 species to our list of those deemed edible, and makes the whole number of New York species of this class 183. Of the 11 added species 9 have been illustrated by colored figures of natural size. Figures of the 2 remaining species, Russula earlei Pk. and Boletus rugosiceps Pk. have been pub- lished in preceding reports. Descriptions of the 11 species tested and approved this year will be found under the title “Edible — fungi.” The study of our Crataegus flora has been continued with much ~ interest. Specimens have been collected in the northern, eastern, central and southwestern parts of the State. The number of species added to the State flora is 8, of which two are new species. This addition makes the number of New York species now known 97. Many specimens of this genus still remain undetermined, The destructive influence of late frosts was clearly seen in the failure of many thorn bushes which bore a full crop of flowers ta REPORT OF THE STATE BOTANIST 1906 7 develop any fruit. Thé essential floral organs were frozen and consequently the fruit failed to develop. In such cases the stamens and pistils are sometimes frozen before the buds open. When the fiowers appear they look fresh and fair at a distance but on close _ inspection the stamens and pistils are seen to be dead and blackened. If the freeze is very severe after the buds are much swollen no species escapes. If less severe, only the flowers of the most tender species or those which are in the most susceptible condition are killed. During the past season many species of the Tomentosae group failed to develop fruit though at flowering time they were full of blossoms. Species in the same locality whose time of flower- ing is earlier may escape injury. The comparatively large genera Hygrophorus and Russula present scme peculiar difficulties. The subgenera are not sharply differentiated and in some cases American species appear to com- bine characters of two subgenera or do not in all respects agree with the characters ascribed to any of the subgenera. Nevertheless a revision of the New York species of these genera has been at- tempted and the Friesian arrangement of the subgenera and species followed as far as possible. Descriptions have been rewritten and in some cases made more full and satisfactory. The plan of identifying specimens of plants for correspondents and others who send or bring them to the office for that purpose has been followed. This not only results in the dissemination of useful botanical knowledge, but also in sometimes acquiring in- teresting and valuable specimens for the herbarium that otherwise might fail to reach it. The number of those for whom determina- tions of specimens have been made is 82. The number of deter- minations is 435. Botanical specimens representing 20 species of trees have been collected but not included-in the foregoing enumeration. They are intended to replace the lost or damaged specimens of the swinging frames, which loss occurred while these were absent at the St Louis and Portland expositions. An additional table case of specimens of parasitic fungi has been prepared and placed in the botanical exhibition room. It contains specimens of 24 species some of which are injurious to cultivated plants, some to wild plants. The case containing the specimens of the Japanese edible mush- foom Shiitake, Pleurotus bretschneideri Kalchb., on the branches where they grew, has been repaired and placed on ex- 8 NEW YORK STATE MUSEUM hibition. It is surmounted by a bell jar filled with the dried mush- rooms in the condition in which they are offered for sale in the markets of China and Japan. Mr S. H. Burnham, the Assistant Botanist, has been chiefly occupied with office work. He has incorporated the collections of 1905 in their proper places, has disinfected and labeled the speci- mens, attended to the correspondence of the office in my absence, identifying specimens sent for determination and giving informa- tion sought concerning them. He has prepared a card catalogue with descriptive references of the new species of fungi described by the State Botanist. = Respectfully submitted . Cuarves H. Peck State Botanist Oftice of the State Botanist Albany, December 26, 1906 REPORT OF THE STATE BOTANIST 1906 SERCIES eA DDED LO tht HERBARIUM New to the herbarium Allionia hirsuta Pursh Amanitopsis pulverulenta Pk. Ascochyta pisi Lib. Aster arcifolius Bu. A. elaeagnus Bu. A. fragrans Bu. A. multiformis Bu. A. violaris Bu. Boletus subpunctipes Pk. Caryospora cariosa Fairm. Collybia campanella Pk. C. lacerata Lasch. Cortinarius intrusus Pk. G validipes Pk. Crataegus arcana Beadle bissellit Sarg. cognata Sarg. deltoides Ashe habereri Sarg. noveboracensis Sarg. scabrida Sarg. : tenella Ashe Cynoglossum boreale Fern. Didymium clavus (4. & S.) Rabenh. Dryopteris pittsfordensis Slo. Entoloma minus Pk. Flammula expansa Pk. Gaura coccinea Pursh Hydnum luteopallidum Schw. Hygrophorus burnhami Pk. aanaaanaa Hygrophorus luridus B. & C. Hypocrea pallida FE. & E. Inocybe pallidipes E. & E. Lepiota asperula Atk. lle eriophora Pk. Leptoglossum fumosum Pk. Linum medium (Planch.) Britton Marasmius phyllophilus Pk. Myeena albogrisea Pk. Nicandra physaloides Gaertn. Ohleria modesta Fckl. Omphalia pusillissima Pk. Panicum deminutivum Pk. Peckiella hymenii Pk. Phyllosticta ampelopsidis FE. & M. 2, sinilacis E. & E. IE sphaeropsidea EL. & E. Pleurotus terrestris Pk. Polyporus galactinus Berk. Puccinia peckii (DeT.) Kell. Russula foetentula Pk. R. modesta Pk. Re pectinatoides Pk. R. vesca Fr. Scleroderma tenerum B. & C. Septoria lycopersici Speg. Steccherinum adustulum Banker Stemonitis smithii Macb. Tricholoma hirtellum Pk. Viola incognita Brainerd Not new to the herbarium Agastache scrophulariaefolia (Willd.) Amanitopsis volvata (Pk.) Sacc. Aquilegia canadensis L. Arctium lappa L. Asarum canadense L. Aster camptilis Bu. A. claytoni Bu. A. concolor L. Boletus auriporus Pk. B. frostii Russ. B. nigrellus Pk. B. peckit Frost Boletus rugosiceps Pk. Bromus tectorum L. Castanea dentata (Marsh.) Borkh. Catastoma circumscissum (B. & C.) Chrysomyxa pyrolae (DC.) Rostr. Chrysopsis mariana Nutt. Clavaria botrytoides Pk. c: cristata Pers. Clitocybe amethystina (Bolt.) (Ce monadelpha Morg. C: ochropurpurea Berk. Clitopilus prunulus (Scop.) Fr. IO NEW YORK STATE MUSEUM Coreopsis rosea Nutt. Cornus alternifolia L. f. (CG; candidissima Marsh. Crataegus caesariata Sarg. coccinea L. ferentaria Sarg. illuminata Sarg. intricata Lange laneyi Sarg. pedicellata Sarg. pringlei Sarg. punctata Jacq. spissiflora Sarg. tenuiloba Sarg. Craterellus cantharellus (Schw.) Cypripedium acaule Ait. Daedalea quercina (L.) Pers. Dasystoma virginica (L.) Britt. Dryopteris boottii (Tuck.) Under. SAAAODAAG © 1D). cristata (L.) Gray 1D). cris. clintoniana (at.) D. simulata Dav. Eleocharis inter. habereri Fern. 18. melanocarpa Torr. Gentiana crinita Froel. Hydnum aurantiacum A. & S. fennicum (Karst.) Sace. imbricatum L. repandum L. vellereum Pk. : zonatum Batsch Hypopitys lanuginosa (Mx.) Nutt. Ilex vert. cyclophylla Robins. Inocybe calamistrata Fr. Irpex canescens Fr. Lactarius ful. fumosus Pk. Le pergamenus Fr. sal ae ass Lactarius piperatus Ir. ile, vellereus Fr. IL, volemus Fr. Lespedeza angustifolia Pursh IL hittas (eS) mele 1 virginica (L.) Britt. Lobelia dortmanna L. Lycopus sessilifolius Gray Meibomia marilandica (L.) Kuntze M. rigida (Ell.) Kuntze Monarda punctata L. Mycena galericulata (Scop.) Physarum lateritium (B. & I. ) Polyporus schweinitzii Fr. 12); sulphureus (Bull.) Polystichum acrostichoides (M-+.) Polystictus simillimus Pk. ie subsericeus Pk. Populus balsamifera L. Russula earlei Pk. Sagina procumbens L. Scirpus atro. pycnocephalus Fern. S. cyp. pelius Fern. Senecio obovatus Muh. Solidago tenuifolia Pursh Sporobolus serotinus (Torr.) Gray Stereum versicolor Fr. Strobilomyces strobilaceus (Scop.) Trillium erect. album Pursh Tricholoma alboflavidum Pk. T. nudum (Bull.) Fr. Viburnum lentago L. Viola blanda [Villd. We cucullata Ait. V. fimbriatula Sm. Woodwardia areolata (L.) Moore CONTRIBUTORS AND? THEIR’ CONTRIBUTIONS Mrs E. B. Blackford, Boston Mass. Lactarius varius Pk. | Omphalia epichysium Pers. Hygrophorus serotinus Pk. Miss M. B. Church, Albany Pleurotus porrigens (Pers.) Fr. Mrs M. S. DeCoster, Little Falls’ Viola incognita Brainerd | \Viola selkirkii Pursh REPORT OF TilE STATE BOTANIST 1906 II Mrs G. M. Dallas, Philadelphia Pa. Opuntia humifusa Raf. Miss Alice Eastwood, San Francisco Cal. Lentinus magnus Pk. Mrs L. L. Goodrich, Syracuse Trillium erectum album Pursh Mrs M. A. Knickerbocker, San Francisco Cal. Scoliopus bigelovii Torr. Miss EK. A. Lehman, Winston-Salem N. C. Monotropsis lehmanae Burnh. Mrs j. Rogers, Ausable Forks Lepiota naucinoides Pk. Miss A. M. Ryan, New London Ct. Marsonia violae (Pass.) Sacc. Miss T. L. Smith, Worcester Mass. Russula modesta Pk. Mrs F. C. Sherman, Syracuse Pleurotus ulmarius Fr. Mrs C. E. Taft, New York city Collybia velutipes (Curt.) Fr. Mrs E. S. Tomlinson, New York city Polystichum acrostichoides incisum (Gr.) Under. F. H. Ames, Brooklyn Ammodenia peploides (L.) Bupr. | Hudsonia tomentosa Nutt. Woodwardia areolata (L.) Moore J. C. Arthur, Lafayette Ind. Aecidium coloradense Diet. | Peridermium boreale Arth. Peridermium carneum (Bosc) S. & E. G. F. Atkinson, Ithaca Cortinarius intrusus Pk. | Lepiota asperula Atk. Russula constans Karst. 12 NEW YORK STATE MUSEUM H. J. Banker, Greencastle Ind. Onygena equina Pers. | Steccherinum adustulum Banker Elam Bartholomew, Stockton Kan. Aecidium abundans Pk. Ae. allenii Clint. Ae. diodiae Burr. Ae. grindeliae Griff. Ae. grossulariae (Pers.) Sch. Ae. pammelii Tyel. INE punctatum Pers. Ae. solidaginis Schw. Albugo amaranthi (Schw.) Kee. A. candidus (Pers.) Kee. Arthosporium compositum 4. Cercospora pachypus £. & K. C. vignae HE. & E. Coleosporium solidaginis (Schw.) Coniosporium arundinis (Cd.) Sacc. Cronartium asclepiadeum Berk. Cucurbitaria salicina Fckl. Cudonia circinans (Pers.) Fr. Diplodia liriodendri Pk. Dothidea linderae Ger. Exobasidium vaccinil (Fckl.) Wor. Geaster pectinatus Pers. Geoglossum hirsutum Pers. G. peckianum Che. Gymnosporangium clavipes C. & P. Humaria cestrica E. & E. Hypomyces lactifluorum (Schw.) Tul. Leotia lubrica (Scop.) Pers. Meliola nidulans (Schw.) Che. Mitrula olivacea (Pers.) Sacc. M. serpentina (Muell.) Mass. Oidium monilioides Lk. Peronospora calotheca DeBy. Ps euphorbiae Fckl. Phyllachora graminis panici (Schw.) Plasmopara geranii (Pk.) B. & DeT. Psilocybe sabulosa Pk. Puccinia absinthi DC. agropyri LE. & E. asparagi DC. asteris Duby caricis (Schum.) Reb. cyperi Arth. ge rele aca ae Macrosporium ornatissinum EF. & B. Marsonia castagnei (D. & M.) Sacc. Massariella bufonia (B. & Br.) Tul. Puccinia fraxinate (Lk.) Arth. helianthi Schz. heucherae (Schw.) Diet. lycii Kalchb. menthae Pers. muhlenbergiae A. & H. physalidis Pk. pimpinellae (Strauss.) Lk prenanthis (Pers.) Fckl. proserpinacae Farl. purpurea Cke. rubinella (Pers.) Arth. silphii Schw. stipae Arth. fecha Ex sorb tosta Arth. verbesinae Schw. veroniae Schw. Rhizographus fusariisporus E. & E. Rhizopus nigricans Ehrenb. Schizothyrella fraxini E. & E. Sclerospora graminicola (Sacc.) Scolecotrichum asclepiadis E. & E. Septoria aurea destruens FE. & E. S. munroae FE. & B. Sorosporium syntherismae (Pk.) Farl. Sphaeropsis cydoniae C. & E. Stichopsora solidaginis (Schw.) Dict. Teichospora populina FE. & E. Tricholoma portentosum Fr. Tubercinia clintoniae Kom. Tuberculina persicina (Ditm.) Sacc. Typhula muscicola (Pers.) Fr. pe a eee eet Uromyces caladii (Schw.) Farl. U. euphorbiae C. & P. U gentianae Arth. U elycyrrhizae (Reb.) Magn. WU. enaphalii £. & E. WwW, * hordei Tracy U. howei Pk. U. junci (Desm.) Tul. U lespedezae (Schw.) PR. UW. trifolii (Hedw.) Lev. Ustilago utriculosa (Nees) Tul. Xylaria digitata (L.) Grev. REPORT OF THE STATE ROTANIST 1906 13 M. S. Baxter, Rochester Crataegus laneyi Sarg. Crataegus tenuiloba Sarg. . pedicellata Sarg. Pentstemon laevigatus Soland. : M. S. Baxter and V. Dewing, Rochester Allionia hirsuta Pursh | Gaura coccinea Pursh Conringia orientalis (L.) Dui. R. C. Benedict, New York city Dryopteris pittsfordensis Slosson A. F. Blakeslee, Cambridge Mass. Phycomyces nitens (Ag.) Kunze F. S. Boughton, Pittsford Clitocybe dealbata Soz. | Pleurotus subareolatus Pk. Tricholoma columbetta Fr. F, J. Braendle, Washington D. C. Clavaria cinerea Bull. Isaria truncata Pers. Collybia zonata Pk. Mycenastrum spinulosum Pk. Geaster saccatus Fr. Viola villosa Wali. S. H. Burnham, Sandy Hill Cordyceps capitata (Holmsk.) Lk. Pleurotus terrestris Pk. Cynoglossum boreale Fern. Polyporus borealis Wahl. Erysiphe polygoni DC. Polystichum acrostichoides (Mv+.) Flammula expansa Pk. Russula cyanoxantha (Schaeff.) Fr. Hygrophorus burnhami Pe. Scapania irrigua (Nees) Dum. Lentinus spretus Pk. Timmia megapolitana Hedw. Lepiota asperula Atk. G. H. Chadwick, Albany Thelephora schweinitzil Pk. G. D. Cornell, Coopers Plains Arabis glabra (L.) Bernh. Liriodendron tulipifera L. Hieracium praealtum Jill. Magnolia acuminata L. Hypericum ascyron L. Solidago juncea Ait. Lilium canadense L. Sisyrinchium angustifolium Mill. W. C. Cottrell, Gloversville Nicandra physaloides Gaertn. 14 NEW YORK STATE MUSEUM Simon Davis, Brookline Mass. Agaricus camp. hortensis Cke. Coprinus plicatilis Fr. C. stenocoleus Lindb. Eccilia unicolor Pk. Entoloma sericellum Fr. E. sericeum (Bull.) Fr. Galera sphagnorum Pers. Hygrophorus davisii Pk. Hygrophorus luridus B. & C. Tal. mephiticus Pk. le nitratus (Pers.) Fr. Tel, prat. albus Sacc. Inocybe infelix Pk. Leptonia transformata PR. Marasmius scorodonius Fr. Psathyrella angusticeps Pk. Russula compacta Frost W. T. Davis, New Brighton Aronia arbutifolia (L.) Medic. | Aronia atropurpurea Britton Frank Dobbin, Shushan Arthonia radiata (Pers.) Th. Fr. Discina orbicularis Pk. Arthonia quintaria Ny. Philip Dowell, Port Richmond Dryopteris boottii (Tuck.) Under. Dryopteris goldieana (Hook.) Gray D. cristata (L.) Gray D. pittsfordensis Slos. D. crist. clintoniana (Eat.) D. simulata Dav. 1D), crist. marginalis Dav. Woodwardia areolata (L.) Moore C. E. Fairman, Lyndonville Brachysporium obovatum (Berk.) Sace. Caryospora cariosa Fairm. Didymium clavus (A. & S.) Rabh. Nemosphaeria fairmani Sacc. Ohleria modesta Fckl. O. E. Fischer, Detroit Mich. Agaricus camp. hortensis Cke. | Lepiota eriophora PR. Hydnum adustum, Sch. N. M. Glatfelter, St Louis Mo. Guepinia palmiceps Berk. Merulius rubellus Pk. Lepiota cep. lutea With. Pterula densissima B. & C. Thelephora caespitulans Schzw. P. W. Graff, Storrs Ct. Poronia macrospora Pk. Xylaria polymorpha combinans Pk. Cephas Guillet, Toronto Ont. De 5 P : Hygrophorus miniatus Fr. | Lactarius paludinellus Pr. | Physarum lateritium (B. & R.) Rost. REPORT TOD Tih SLADE SOLANISD 1906 C. C. Hanmer, East Hartford Ct. Collybia lacerata Lasch. Hygrophorus chlorophanus Fr. Entoloma cuspidatum Pk. Panus levis B. & C. M. E. Hard, Chillicothe O. Hydnum ochraceum Pers. | Tricholoma fumescens Pk. J. J. Hare, Whitby Ont. Hypholoma sublateritium squamosum Cke. J. E. S. Heath, South Pasadena Cal. Daldinia vernicosa (Schw.) C. & D. A. P. Hitchcock, New Lebanon Lycoperdon giganteum Batsch G. S. Howell, Rockville Ind. Tricholoma album Schaeff. C. H. Kauffman, Ann Arbor Mich. Crepidotus ralfsii B. & Br. Lepiota gracilis Pk. Cortinarius multiformis Fr. Mycena glutinipes Kauff. Hypholoma vinosum Kauff. Pleurotus petaloides (Bull.) Fr. W. A. Kellerman, Columbus O. Galera kellermani Pk. | Psathyrella hirta Pk. F. D. Kern, Lafayette Ind. Puccinia graminis Pers. R. B. Mackintosh, Peabody Mass. Agaricus campester L. | Agaricus rodmani Pk. Charles McIlvaine, Cambridge Md. Lepiota morgani PR. George E. Morris, Waltham Mass. Hygrophorus pallidus Pk. Lepiota eriophora Pk. iT ruber Pk. Steccherinum adustulum Banker L. J. Muchmore, Batavia Hydnum luteopallidum Schw. | Oligonema nitens (Lib.) Rost. Stemonitis smithi1 Macb. 5 16 NEW YORK STATE MUSEUM F. M. Rolfs, Mountain Grove Mo. *Phyllosticta rubra Pk. W. H. Ropes, Salem Mass. Agaricus micromegethus Pk. I. M. Shepherd, Trenton, N. J. Morchella esculenta (L.) Pers. F. S. Smith, Angelica Bacillus amylivorus Burr. | Fusicladium pirinum (Lib.) Fckl. Perley Spaulding, St Louis Mo. Merulius lac. verrucifer Quel. M. rubellus Pk. Fomes annosus Fr. Iiydnum artocreas Berk. E. B. Sterling, Trenton N. J. Arachnion album Schw. Lycoperdon tessellatum Lloyd Calostoma cinnabarinum Desv. Pholiota discolor Pk. Inocybe sterlingii Pk. Pluteus petasites Fr. Lycoperdon excoriatum Lloyd i Sarcoscypha dawsonensis Pk. ie pusillum Batsch | Scleroderma aurantiaca Pers. IL. serotinum Bon. Shee cepa Pers. Ibe stellare (Pk.) Lloyd | S verrucosum ( Bull.) D. R. Sumstine, Wilkinsburg Pa. Pyronema leucobasis (Pk.) Sacc. Hermann von Schrenk, St Louis Mo. Paxillus panuoides Fr. | Trametes serialis Fr. K. F. Symonds, Utica Clitocybe ochropurpurea Berk. E. A. White, Storrs Ct. Phallogaster whitei Pk. T. E. Wilcox, Washington D. C. Boletus retipes B. & C. Clavaria pistillaris L. B. rimosellus Pk. Collybia strictipes Pk. B. subtomentosus L. Hymenogaster anomalus /°R. Tricholoma columbetta Fr. W. W. Eggleston, New York city By exchange Crataegus arcana Ashe Crataegus deltoides Ashe GC, coccinea L. " C. dissona Sarg. €: cognata Sarg. Cc dodgei Ashe REPORT OF THE STATE BOTANIST 1906 7 Crataegus glaucophylla Sarg. Crataegus modesta Sarg. @ intricata Lange C. pentandra Sarg. ec. matura Sarg. C. pruinosa [IV endl. Crataegus tenella Ashe SEECins NOR BEFORE REPORTED Allionia hirsuta Pursh Near Rochester. August. M.S. Baxter and V. Dewing. Intro- duced from the western states. It is Oxybaphus hirsutus Sweet. Amanitopsis pulverulenta n. sp. Pileus thin, convex beceming nearly plane, pulverulent, squamose in the center, even on the margin, white or creamy white, odor feeble or none; lamellae thin, unequal, narrowed behind, free or nearly so, moderately close, subventricose, whitish; stem equal or slighfly tapering upward, bulbous, solid, pulverulent or fur- furaceous, white; spores subelliptic, .oo03-.0004 of an inch long, .0002~.00024 broad. Pileus 1-2 inches broad; stem 1-2 inches long, 2-3 lines thick. Shaded banks by roadsides. Port Jefferson, Suffolk co. August. This species is well marked by its white color and the copious mealiness of the pileus and stem. It is apparently closely related fo Amanitopsis pubescens (Schw.) but-it differs from the description of that species in having the pileus and stem pul- verulent instead of pubescent and in the former being squamose in the center. There is no annulus and the slight remains of a mem- Dranous volva are seen in very young specimens only. In the dried specimens the lamellae have assumed a pale yellowish cinnamon hue. Ascochyta pisi Lib. Living pods of peas and beans. Menands, Albany co. July. This. parasitic fungus produces discolored spots on the pods similar to the anthracnose spots of bean pods, but the spores of this fungus are uniseptate, those of the anthracnose, simple. | Aster arcifolius Bu. Lake Minnewaska, Ulster co. September. Prof. E. Burgess has made a special study of the asters of our country and his re- vision and elucidation of the Biotian division of the genus enables 18 NEW YORK STATE MUSEUM me to add to our New York flora several species which were formerly supposed to be varieties of Aster divaricatus, A. macrophyllus and other closely related species. Aster biformis Bu. Rathboneville, Steuben co. and Voorheesville, Albany co. August and September. In this species the lower stem leaves are petiolate and cordate with a deep narrow sinus, the upper leaves are abruptly reduced to a smaller size and are nearly or quite sessile. This dif- ference between the upper and lower leaves is suggestive of the specific name. Aster camptilis Bu. Low rocky ground. Lake Minnewaska. September. A slender aster with a weak stem which is often reclined or bent as if too feeble to support its own branches or hold itself erect. This char- acter is suggestive of the name bent stemmed aster. Aster claytoni Bu. Open places. Menands, Albany co. September. A large and variable species belonging to the group Divaricati. Specimens are sometimes 3 feet tall. ° Aster elaeagnus Bu. North Elba, Essex co. August. A northern species having orbicular or ovate radical leaves and variable stem leaves which are pale and hairy on the under side. This gives a scurfy appearance suggestive of the scurfy character of Elaeagnus leaves. The species belongs to the group Macrophylli. Aster fragrans Bu. Round Lake, Saratoga co. September. This species differs from A. divaricatus,. to which it was formerly referred, in its more persistent fragrance, more compact panicle of flowers and more truncate base of its leaves. Aster multiformis Bu. Lake Minnewaska, Ulster co. September. A species remark- able for its long slender rootstocks and the many forms shown by the leaves of the same plant. REPORT OF THE STATE BOTANIST 1906 1g9) Aster violaris Bu. Rathboneville, Steuben co. August. This species is distin- guished by its suborbicular and reniform apiculate radical and lower stem leaves. It belongs to the group Macrophylli. Boletus subpunctipes n. sp. Pileus fleshy, broadly convex, often uneven on the surface, be- coming soft with age, brown, reddish brown when dry, flesh white, slowly becoming dingy where cut or broken, taste mild; tubes nearly plane in the mass, adnate or but slightly depr2ssed around the stem, the mouths small, round, whitish or grayish white, chang- ing to reddish brown where wounded; stem equai or nearly so, solid, slightly reticulate at the top, very minutely dotted, some- times obscurely squamulose at the top, grayish or pallid; spores rusty brown or cinnamon brown, oblong or subfusiform, .ooo4~ 0005 of an inch long, .0002—.00024 broad. Pileus 2-4 inches broad; stem 2-3 inches long, 4-6 lines thick. Shaded sandy soil. Menands, Albany co. August. The surface of the pileus is rendered uneven by coarse shallow depressions. The species belongs to the section Versipelles. The dots on the stem are nearly like those on the stem of Boletus mir Oomapes Frost. Caryospora cariosa Fairm. In cavities of oid beech wood. Lyndonville, Orleans co. C. E. airman. Collybia campanella n. sp. Pileus thin, conic or campanulate with a papilla at the apex, covered with coarse appressed or deflexed strigose hairs, dark tawny; lamellae ascending, moderately close, whitish; stem firm, equal, inserted, floccose hairy, colored like the pileus; spores not seen. Pileus 3-4 lines broad; stem 9-12 lines long, .5 of a line thick. ead and dry branches of arbor vitae, Thuja occidentalis. Horicon, Warren co. July. Siticmcpecies 1s related to Collybia stipitaria from which it is readily distinguished by its persistently conic or cam- panulate pileus and its uniformly dark tawny color of both pileus and stem. The hairy tufts of the stem are pointed and project at right angles from the stem. 20 NEW YORK STATE MUSEUM Collybia lacerata Lasch. Dry soil among grasses and bayberry bushes. Fishers island, Suffolk co. October. C. C. Hanmer. In these specimens the ex- panded pileus is umbonate and the umbo is darker colored than the rest. The specimens agree well with the figure of the species as given in Cooke’s Illustrations of British Fungi. The spores in our specimens are broadly elliptic or subglobose and .00024—.0003 of an inch long. Cortinarius intrusus Pk. Carnation beds in greenhouses. Highland Falls, Orange co. January. Ernest Palmer. Communicated by G. F. Atkinson. The species was described from specimens found growing in mush- room beds in conservatories in Massachusetts and New Jersey and communicated by R. Macadam and C. Mclivaine. Cortinarius validipes n. sp. Pileus fleshy, thick, convex becoming nearly plane, dry, squamu- lose or floccose squamulose, ochraceous, flesh white tinged with yellow next the lamellae, taste mild; lamellae thin, narrow, close, adnate or decurrent with a tooth, yellowish white becoming cinna-_ mon; stem stout, firm, solid, fibrous, striate at the top by the de- current teeth of the lamellae, subannulate from the adherent re- mains of the webby veil, yellowish white, whitish within; spores subeiliptic, .o003—.0004 of an inch long, .0002~.00024 broad. Pileus 3-6 inches broad; stem 4-5 inches long, 1-2 inches thick. © Coopers Plains, Steuben co. September. A cluster of six plants was found growing in a small excavation near a farmhouse. The weather had been unusually warm and dry for several weeks, but a soaking rain two days before and a thunder shower one day later seem to have been favorable to the © development of this large fine mushroom. It belongs to the section Dermoeybe. Crataegus arcana Beadle : Moores Mills, Dutchess co. May and October. W. W. Eg-7 eleston. Crataegus bissellii Sarg. J ie > Rocky pasture, near Staatsburg, Dutchess co. May and Septem- { ber. Our plants differ from the typical form of the species only — in having stamens 5-8 and anthers pale pink soon fading to white. 4 j REPORT OF THE STATE BOTANIST 1906 21 Crataegus cognata Sarg. Colemans Station, Dutchess co. and Dykemans, Putnam co. May and September. Mr Eggleston had previously found it in the latter locality. Crataegus deltoides Ashe Moores Mills. May and October. W. W. Eggleston. The broadly ovate or deltoid leaves constitute a prominent feature of this species and are suggestive of the specific name. Crataegus habereri n. sp. Sarg. Leaves broadly ovate, acute, rounded, subtruncate or abruptly cordate at the wide entire or glandular base, finely doubly serrate above, with straight glandular teeth, and divided usually only above the middle into four or five pairs of small acuminate spreading lobes, nearly half grown when the flowers open about the middle of May and then membranaceous, light yellow green and roughened above by short white hairs and pale and glabrous below, and ‘at maturity thin, dark yellow green and scabrate on the upper surface, light yellow green on the lower surface, 4.5-6.5 cm long and nearly as wide; with slender midribs, and their primary veins extending obliquely to the points of the lobes; petioles slender, slightly wing- margined at the apex, at first slightly villose, soon becoming gla- brous, sparingly glandular while young, 2.5—3.5 cm in length; leaves on vigorous shoots truncate or rounded at the base, more coarsely serrate and more deeply lobed, often 7-8 cm long and 6-7 cm wide. Flowers 1.4-1.5 cm in diameter, on slender slightly hairy pedicels, in broad 5-8-flowered corymbs; calyx tube narrowly obconic, glabrous, or slightly hairy near the base, the lobes slender, acu- minate, glandular serrate, glabrous on the outer, sparingly villose on the inner surface, reflexed after anthesis; stamens 10; anthers dark rose color; styles 3-5, surrounded at the base by a narrow ring of pale tomentum. Fruit ripening from the first to the middle of September, on glabrous reddish pedicels, in few-fruited drooping clusters, oval to obovate, crimson, lustrous, marked by large pale dots ; calyx prominent, with a deep wide cavity, and incurved hori- zontal or recurved lobes dark red above toward the base and slightly hairy on the upper surface, their tips often deciduous from the ripe fruit; flesh thin, dark yellow, soft and succulent; nutlets 3-5, acute at the ends, slightly ridged and irregularly grooved on the back, 7-8 mm long and about 5 mm wide. A shrub 3-5 m high, with small stems, wide spreading flexuous 22 NEW YORK STATE MUSEUM branches, and slender slightly zigzag glabrous branchlets, light orange greet’ when they first appear, becoming light chestnut- brown, lustrous and marked by pale lenticels in their first season, and dul! reddish brown the following year, and armed with slender straight or slightly curved chestnut-brown spines 2.5—3 cm long. Rocky pastures and margins of woods; New Hartford, Oneida co. J. V. Haberer (4 2410, type), May 20 and September 28, 1903; (Co isl, PEO, Seoursmose wir, usec, This species, remarkable in its broad slightly lobed leaves and early ripening fruit, is named for its discoverer, Joseph Valentine Haberer M. D., an enthusiastic student of the flora of Herkimer, Oneida and Madison counties, the founder of the Asa Gray Botanical Club of Utica in 1886 and from that time to the present its president. Crataegus noveboracensis n. sp. Sarg. Leaves ovate, acuminate, abruptly concave cuneate at the entire base, finely doubly serrate above, with straight glandular teeth, and deeply divided into five or six pairs of narrow acuminate spreading lobes, more than half grown when the flowers open at the end of May and then thin, yellow green and covered above by short soft white hairs and paler and glabrous below, and at maturity thin but firm in texture, dark yellow green and lustrous on the upper surface and pale yellow green on the lower surface, 4.5-6.5 cm long and ~ 4-5 cm wide, with slender yellow midribs, and thin primary veins arching obliquely to the points of the lobes; petioles slender, slightly wing-margined at the apex, villose on the upper side while young, — becoming glabrous, sparingly glandular, 1-2 cm in length; leaves j on vigorous shoots thicker, sometimes rounded or subtruncate at — the broad base, more coarsely serrate and more deeply lobed, often — 7-8 cm long and 6-7 cm wide, with stouter broadly winged petioles. _ Flowers 1.2-1.4 cm in diameter, on slender slightly villose pedicels, © in usually 7-11-flowered lax corymbs; calyx tube narrowly obconic, coated especially near, the base with long scattered white hairs, the lobes gradually narrowed, slender, acuminate, glandular serrate, glabrous on the outer, villose on the inner surface, reflexed after anthesis; stamens 15-20; anthers pale yellow; styles 4 or 5. Fruit ripening the middle of September, on slightly hairy reddish ped- icels, in usually 5—7-fruited drooping clusters, subglobose to short oblong, full and rounded at the ends, crimson, lustrous, marked by | large pale dots, about 1 cm in diameter; flesh thin, yellow, dry and ; mealy; nutlets 4 or 5, narrowed) and rounded at the ends, slightly | REPORT OF THE STATE BOTANIST 1906 23 ridged on the back, with a low slightly grooved ridge, 5.5-6 mm long and 4-5 mm wide. A shrub 3-4 m high, with numerous small stems, ascending or suberect branches and slender nearly straight glabrous branchlets dark orange green when they first appear, becoming light chestnut- brown, lustrous and marked by pale lenticels in their first season and light gray brown the following year, and armed with numerous slender straight or slightly curved light chestnut-brown shining spines 4-5 cm long. Sandy or rocky soil; Essex co. Common. North Elba, C. H. Peck (# 40, type), May 27, July 22 and September 14, 1903; Met Peck ( 40), Keene, May 31 and September 16, 1903. Crataegus scabrida Sarg. Hilly and rocky pastures. West Albany, Albany co., C. H. Peck; New Hartford, Oneida co., J. V. Haberer. May and September. This is a large shrub or small tree which occurs in several places about Albany. It also occurs in Petersburg, Rensselaer co. Its fruit is edible. Crataegus tenella Ashe Hilly and rocky pastures. Colemans Station and Moores Mills, Dutchess co.; Dykemans, Putnam co. May, September and Octo- ber. W. W. Eggleston. Cynoglossum boreale Fern. West Fort Ann, Washington co. June. S. H. Burnham. Didymium clavus (A. & S.) Rabenh. _ Dead herbaceous stems. Grove Springs near Lake Keuka. July. C.E. Fairman. These specimens differ from typical forms in having a slightiy smaller peridium. Dryopteris pittsfordensis Slosson Springville, Richmond co. May. Philip Dowell. Solway, Onon- daga co. R. C. Benedict. Entoloma minus n. sp. Pileus thin, subconic or hemispheric, becoming broadly convex, glabrous, grayish brown, darker in the center; lamellae thin, close, ascending at first, sinuate behind, whitish becoming flesh color; 24 NEW YORK STATE MUSEUM stem slender, hollow, white; spores subglobose, angular, .0003—.0004 of an inch in diameter. Pileus 8-12 lines broad; stem I-1.5 inches long, about 1 line thick. . Ground in woods. East Schaghticoke, Rensselaer co. August, Flammula expansa n. sp. Pileus thin, broadly convex or nearly plane, glabrous or some- times with appressed spotlike scales in the center, subochraceous, flesh white, taste mild; lamellae thin, narrow, close, yellow, changing to brown where wounded; stem short, equal, solid, brownish with- out, yellow within; spores broadly elliptic, .ooo3 of an inch long, .00024 broad. Pileus 1-3 inches broad; stem about 1 inch long, 2-3 lines thick. Decaying wood of red maple, Acer rubrum. Helderbergs, Albany co. July. S. H. Burnham. East Schaghticoke, Rens- selaer co. August. Gaura coccinea Pursh Near Rochester. August. Introduced from the west. M. Se Baxter and V. Dewing. Hydnum coriaceo-membranaceum Schw. Ground. Lake Pleasant, Hamilton co. Hydnum luteopallidum Schw. Decorticated wood and bark of some deciduous tree, apparently butternut, Juglans cinerea. Lyndonville, Orleans co.9 July. L. J. Muchmore. The type specimens of Schweinitz were found on grapevines. In ours the fungus is resupinate, adnate, with a very thin subiculum, smoky yellow or brownish, whitish or pale yellow on the young margin; the teeth are scarcely half a line long, scattered or crowded, sometimes confluent at the base and subfasciculate, colored like the subiculum but white fimbriate at the tips; spores subglobose, colored, verrucose, .ooo16—.0002 of an inch broad. Hygrophorus burnhami n. sp. Ground. West Fort Ann, Washington co. October. The descrip-— : tion of this species may be found in the chapter on New York — Species of Hygrophorus. Hygrophorus luridus B. & C. ‘ Among mosses and fallen leaves in woods. Sand Lake, Rens- selaer co. August. o REPORT OF THE STATE BOTANIST 1906 25 Hypocrea pallida E. & E. On some resupinate polyporoid fungus on oak branches. Lake Minnewaska, Uister co. August. Inocybe pallidipes E. & E. Dead wood and decaying vegetable matter, near Friends lake, Warren co. July. The white stem and brown umbonate pileus are prominent and notable characters of this species. Wood inhabiting species of this genus are few. This one is related to Inocybe euthe- loides Pk. but it is a stouter plant with a thicker, straighter stem which is white even in the dried state. Lepiota asperula Atk. Woods. Near Ithaca. August. G. F. Atkinson. Vaughns, Washington co. July. S.H. Burnham. This last is a form having a more slender stem and slightly darker pileus, but scarcely worthy of specific distinction. Lepiota eriophora Pk. Jamestown, Chautauqua co. August. G. E. Morris. This is distinguished from the preceding species by its smaller size, darker brown color, denser crowded scales of the pileus and specially by the copious brown tomentum of both pileus and stem, a character Suggestive of the specific name. It has not yet been found in the eastern part of the State. Its range is apparently westward and southward. Leptoglossum fumosum Pk. Geoglossum luteumfumosum, State Mus. Rep’t 43. 1890. p. 40. Receptacle fleshy, stipitate, oblong, obtuse, terete or compressed and furrowed on one or both sides, glabrous, moist, hollow, distinct from the stem and sometimes with one or two decurrent lobes at the base, 3-6 lines long, 1.5—3 lines broad, smoky yellow ; stem equal or nearly so, glabrous, hollow, about as long as the receptacle, slightly darker ; asci subclavate or cylindric; spores oblong, biseriate, often slightly curved, hyaline, 2-4-nucleate, .oor2—.0016 of an inch long, .00016—.0002 broad. Mossy ground in woods. Sand Lake. August. This was for- merly considered a mere variety of Leptoglossum luteum, but having found a group of good specimens showing well the distinctive characters of the species it seems worthy of specific rank. 26 NEW YORK STATE MUSEUM Linum medium ( Planch.) Britton Hempstead Plains, Nassau co. July. Lycoperdon excoriatum Lloyd Warrensburg, Warren co. October. The specimens referred to this species were found growing about the roots of an old stump in a pasture. They are either scattered or gregarious in their mode of growth. The peridium is grayish brown and umbonate and has a cortex similar to thatof Lycoperdon gemmatum Batsch but it usually separates and falls away in flakes or patches, a char- acter suggestive of the specific name. Sometimes the larger spinules fall away separately, asin L. gemmatum, leaving a scar on the peridium and showing the close telanionehny between the two species. Lycoperdon polytrichum Lloyd Among hair cap mosses, Polytrichum juniperinunmse Piseco, Hamilton co. August and September. Closely related to L. gemmatum, but differing in its peculiar habitat. Lycoperdon serotinum Bon. Decaying wood, old stumps and prostrate trunks of trees. Sep- tember to November. Appearing like a late smooth form of LYy¥CORECCOn jHWieiiGrme Severs Marasmius phyllophilus n. sp. Pileus membranaceous, convex or nearly plane, dry, strongly rugose striate or rugose sulcate, whitish, with a faint pinkish tinge when dry; lamellae narrow, distant, rounded behind, adnexed, white, the interspaces venose; stem tough, slender, equal, inserted, hollow, _ covered with a wince downy or velvety pubescence; spores .0002— .00024 of an inch long, .o0012—.00016 broad. Pileus 4-8 lines broad; stem 10-15 lines long, about .5 of a line thick. Gregarious on fallen leaves in woods. Wading River. Suffolk co. August. Closely related to M. insititius Fr. from which it is sepa- rated by the attachment of the lamellae to the stem and by the white color and pubescent coating of the stem. The spores also are larger than the dimensions of the spores of that species. REPORT OF THE STATE BOTANIST 1906 27 Mycena albogrisea n. sp. Pileus thin, submembranaceous, ovate or subcampanulate, obtuse, elabrous, sulcate striate, grayish white ; lamellae rather thick, broad, distant, adnate, colored like the pileus; stem slender, glabrous, hollow, paler than the pileus, with a whitish strigose villosity at the base; spores .0003 of an inch long, .ooo16-.0002 broad. Pileus 3-5 lines broad, nearly as long; stem 1-2 inches long, about half a line thick. Attached to fallen leaves of coniferous trees. Bolton, Warren co. September. It belongs to the section Basipedes. In the dried specimens the pileus has assumed a slightly darker or smoky tint, but it still retains its sulcate striate character. Nicandra physaloides Gaertn. Gloversville, Fulton co. September. W. C. Cottrell. Introduced from Peru. The common name of its fruit 1s apple of Peru.» In Illustrated Flora of the Northern States and Canada its name is Sivenas Physalodes physalodes (L.) Britton, but the International Botanical Congress having decided against the use of double names, we have used the name given in Gray’s Manual. Omphalia pusillissima n. sp. Pileus membranaceous, broadly convex or nearly plane, glabrous, umbilicate, slightly striate on the margin when dry, white; lamellae few, distant, decurrent, white; stem slender, filiform, flexuous, glabrous, white; spores subglobose or broadly elliptic, .ooo2-.00024 of an inch long, .00016—.0002 broad. Pileus 1-2 lines broad; stem 3-5 lines long. On humus and decay- - ing twigs under pine trees. Delmar, Albany co. August. This is one of the smallest species of Omphalia known to me. The lamellae are very narrow, sometimes branched and sometimes absent. It is a smaller mushroom than Omphalia inte- gtella, and differs from it in its umbilicate pileus. The stem is holiow but the cavity is minute. Ohleria modesta Fckl. On carious wood of beech. Lyndonville, Orleans co. March. ee. Fairman. Panicum deminutivum n. sp. Culms 4-10 inches tall, slender, erect, branched, slightly hairy near the base; branches 3-6, short, suberect, each terminating in a 28 NEW YORK STATE MUSEUM panicle, occasionally bearing one or two branchlets; radical leaves lanceolate, sparingly villose, 3-6 lines long, cauline leaves narrowly lanceolate or linear, acuminate, 6-12 lines long, 1-1.25 lines broad, minutely pubescent beneath, glabrous above, or one or two lower ones sometimes with a few long scattered hairs, the sheaths mostly shorter than the internodes and minutely pubescent, stipules a tuft of slender bristlelike hairs .5-1 line long; panicles ovate in outline, 6-12 lines long, the branches and pedicels glabrous, spikelets sub- globose or oval, less than .5 of a line long, the first scale minute, glabrous or nearly so, second and third scales nearly equal in length, minutely pubescent, the second commonly purplish. Moist or wet muddy soil. Shore of Little pond about 2.5 miles south of Wading River, Suffolk co. August. This diminutive panic grass has smaller spikelets than any species I find described. In most of its characters it approaches closely to Panicum psammophilum Nash from which I have separated it because of the smaller size of all its parts, its different mode of growth and different habitat. This is wet humus or decomposed vegetable matter which is apparently submerged in times of high water. The mode of growth is scattered, not cespitose, and the pubescence except at tae base of the stem is so minute that it is scarcely visible to the naked eye. Unless carefully examined with a magnifying glass the plants would be considered glabrous. Peckiella hymenii n. sp. Subiculum white, overrunning the hymenium of the host plant ‘and obliterating the lamellae, sometimes interrupted; perithecia minute, globose, semiimmersed in the subiculum, numerous, pale honey color becoming darker with age; asci linear, .oog—.013 of an inch long, .0003-.0004 broad; spores monostichous, fusiform, acute at each end, hyaline, .oor6é—o018 of an inch long, .00025—.0003_ broad, oozing from the perithecia and forming irregular whitish” masses upon them, On the hymenium of Lactarius vellereus Fr Wade ing River, Suffolk co. August. The parasite in all the specimens seen, is limited to the hymenium of the host plant, the upper surface of the pileus and the stem remaining unchanged. The host plant also retains its acrid taste. The perithecia are so numerous that they give a general pallid hue to the parasite, though the subiculum itself is white. The emitted spores, adhering in minute masses, do not cover the surface. with Pextdies = = REPORT OF THE STATE BOTANIST 1906 29 a white pulverulence as the spores of the related Hypomyces Meetitluorum (Schw.) Tul. do. Peramium tessellatum (Lodd.) Rydb. Woods. Floodwood, Franklin co. North Elba, Essex co. August. This may be.separated from Peramium repens (L.) Salisb. by its spiral arrangement of the flowers of the spike. Peridermium consimile A. & Kk. Living leaves of spruce trees. Common in the swamps and on the mountains of the Adirondack region where it is associated with Peridermium decolorans Pk. from which it may be dis- tinguished by its smaller spores. Phyllosticta ampelopsidis E. & M. Living leaves of woodbine, Ampelopsis quinquefolia. Wading River, Suffolk co. August. Phyllosticta smilacis E. & E. imine leaves of greenbrier, Smilax rotundifolia Mx. Wading River, Suffolk co. August. Phyllosticta sphaeropsidea E. & E. Living leaves of horse chestnut, Aesculus hippocas- meecum 1. Port Henry, Essex co. September. Pleurotus terrestris n. sp. Pileus thin, broadly convex, even, glabrous, moist, whitish; la- mellae thin, close, broad, slightly emarginate, adnexed, whitish; stem equal, even, curved, glabrous, solid; eccentric, whitish; spores white, globose, .0o0028-.00032 of an inch broad. Pileus 2-3 inches broad; stem 2-3 inches long, 3~4 lines thick. Cespitose. On the ground in the margin of woods, West Fort Ann, Washington co. October. S. H. Burnham. ‘This species belongs to the section Eccentrici, group Tricholo- atarii, Polyporus galactinus Berk, Trunks of apple trees. Delmar, Albany co. August. The fresh oung specimens are white, but in drying they assume a pale straw lor which in time becomes a dingy yellow. The spores in our xamples are subglobose, .00916—.0002 of an inch broad, 30 , NEW YORK STATE MUSEUM Puccinia peckii (DeT.) Kell. On hairy fruited sedge, Carex trichocarpa. North Greenbush. This is the teleutospore form. The aecidial form occurs on living leaves of evening primrose, Onagra biennis (L.) Scop. This form occurs in summer, the other in autumn. Russula foetentula Pk. The description of this species may be found in the chapter on “New York Species of Russula.”’ Russula modesta Pk. For description see chapter on “ New York Species of Russula.” Russula pectinatoides Pk. : The description of this species may be found in the chapter on “ Edible Fungi.” Russula vesca Fr. Woods. Bolton Landing, Warren co. August. Scleroderma tenerum B. & C. This is a small Scleroderma, scarcely attaining a diameter of 1 inch, and having a thin grayish or grayish yellow peridium spotted by very smail appressed brownish scales. It is gregarious or some- times cespitose in its mode of growth. It is not rare, but has been confused with another species both in this country and in Europe, Septoria lycopersici Speg. Living leaves of tomato. Menands. July. This parasitic fungus produces spots on the leaves and finally discolors the whole leaf and kills it. It is an injurious species. Stecchérinum adustulum Banker ; On dead wood and sticks. Jamestown, Chautauqua co. G. E. Morris. East Schaghticoke, Rensselaer co. July. H. J. Banker. Thisil species differs from the common Hydnum.adustum Schw. or its equivalent Steccherinum adustum Banker, in its smaller size and its persistently white or whitish pileus and spines or teeth. Its spores are also a little shorter than in that species. REPORT OF THE STATE BOTANIST I906 31 Stemonitis smithii Macb. Decaying wood. Lyndonville, Orleans co. July. L. J. Muchmore. Tricholoma hirtellum n. sp. On or about pine stumps. Wading River, Suffolk co. August. The description of this species may be found in the chapter on “ Edible Fungi.” Viola incognita Brainerd Damp or moist ground. Little Falls. Mrs M. S. DeCoster. Sand Lake, Rensselaer co. May. NEN E XOMRALIMITAL, SPECIES OF FUNGI Phallogaster whitei Peridium subglobose, 4-5 lines broad, abruptly contracted below into a cylindric stem about 4 lines long and 1 line thick, stellately or radiately rupturing when mature, the rays recurved; glebe masses greenish, becoming black in drying, separated from each other by a white slightly lobed columella, the lobes not reaching the inner surface of the peridium; spores minute, oblong, .ooo16-.0002 of an inch long. Much decayed wood. Storrs, Ct. July. E. A. White. Closely allied to Phallogaster saccatus Morg. but distinct in its smaller size, differently shaped peridium, different mode of rup- ture, more distinct cylindric stem and different internal structure. Like that species it has an abundance of white branching mycelial strands. It is dedicated to its discoverer. Hymenogaster anomalus Peridium thin, subglobose, 9-12 lines in diameter, glabrous, slightly lacunose, often with a rootlike strand of mycelium at the base, whitish, sometimes tinged with red above, white and cellular within, the cells empty, .5-1 line in diameter, sterile base obsolete or nearly so, odor slight, not disagreeable; spores globose or broadly elliptic, even, hyaline, uninucleate, .ooo4—.00055 of an inch long, 00035-.0005 broad. Near Washington, D. C. August and September. T. E. Wil- cox. This species is most closely related to Hymenogaster thwaitesii B. & Br. by its subglobose spores, but it may be separated by its white substance, its smoother colorless spores and ah | as 32 NEW YORK STATE MUSEUM ele, ISS ee ees its cordlike strand of mycelium. This last character is unusual this genus and suggestive of the specific name, z Yeh Ss Leptonia transformata Pileus thin, submembranaceous, slightly convex or nearly plane, often umbilicate, silky tomentose, dry or slightly moist in wet weather, striatulate on the margin which is at first incurved, some- times becoming wavy or split when old, white, flesh white, taste farinaceous; lamellae sinuate, adnexed, close, unequal, ventricosel white becoming pink; stem long, slender, straight or flexuose, equi or slightly narrowed upward, pruinose at the top, glabrous and shining below, subcartilaginous, stuffed or hollow, white with a white mycelium at the base; spores flesh colored, angular, unind- cleate, .0004-.0005 of an inch long, .0003-.00035 broad. Pileus 5-10 lines broad; stem 1-2 inches long, .5-1 line thick. Bushy places. Falmouth, Mass. July. S. Davis. Both pileus and stem become blackish or blackish brown in drying and the pileus becomes deeply umbilicate and strongly striate from the margin to the umbilicus. These changes give the dried plant an appearance quite unlike that of the fresh one. Hygrophorus ruber Pileus thin, conic, commonly unexpanded, acute or subobtuse, cuspidate or narrowly umbonate, very viscid or glutinous, bright red, not turning black in drying; lamellae narrow, ascending, ad- nexed, subdistant, yellow or Siowien brown; stem equal, viscid, hollow, colored like the pileus; spores subelliptic, .00024—.0003 of an inch long, .o0016—.0002 broad. “i Pileus .5-2 inches broad; stem scarcely 1 inch long, 1 line thick. Among mosses in wooded swamps. Ellis, Stow, Cohasset, Mass. September. G. E. Morris. 4 Distinct from H. conicus in its usually smaller size, more viscid pileus, bright red stem and persistent unchanging’ color in | drying Hygrophorus serotinus Pileus fleshy but thin, convex or nearly plane, often with the thin margin curved upward, glabrous or with a few obscure innate fibrils, reddish in the center, whitish on the margin, flesh white, taste mild; lamellae thin, subdistant, adnate or decurrent, white, the interspaces slightly venose; stem equal, stuffed or hollow, glabrous, whitish; spores white, elliptic, .oo03 of an inch long, .0002 broad. — re ; " | 5 REPORT OF THE STATE BOTANIST 1906 33 Pileus 8-15 lines broad; stem about 1 inch long, 52:5 olines thick. Gregarious or cespitose in woods of oak and pine. Shore of Hammond pond near Boston, Mass. November. Mrs E. B. Black- ford. This species is similar in size and color to H y grophorus queletii Bres. but that species is described as haying the margin ef the pileus viscid when young and adorned with white flocci, the center of the pileus covered or spotted with reddish squamules or flocci and at length rimose areolate, the lamellae tinged with citrine yellow, the stem solid and furfuraceous or squamulose and the habitat is said to be larch woods only. None of these characters is applicable to our plant. It also resembles H. subrufescens Pk. in size and color but it differs from it in its more glabrous pileus with paler margin, its white flesh, stuffed or hollow stem and later time of appearance. This last character is suggestive of the name given io the species. Xylaria polymorpha combinans n. var. Club subglobose, often compressed and irregular, cespitose at the top of a common subterranean stem or of two stems united at the top; perithecia and spore character as in the species. Growing from roots of a dead maple tree. Bridgeport, Ct. November. P. W. Graff. The subterranean stem is about 2a inches long. the clubs 1-1.5 broad. The clubs appeared as if resting on the ground. The subglobose shape of the club or stroma is char- acteristic of X. polymor pha hypoxylea Nits. and the ces- pitose mode of growth, of X. polymorpha spathulata Pers. This combination of characters of two varieties in one is Suggestive of the varietal name here given. REMARKS AND OBSERVATIONS Agastache scrophulariaefolia (Willd.) Kuntze This is a very variable species. A peculiar form occurs near Port Jefferson, in which the leaves are abruptly acuminate or cus- pidate and the upper ones are entire or nearly so. The flower spikes are more narrow than usual and are sometimes interrupted toward he base. Boletus nigrellus Pk. A form of this extremely rare species was found in Sand Lake in Which the pileus is yellowish or greenish yellow when fresh, and 34 NEW YORK STATE MUSEUM its flesh, as well as the tubes and stem, slowly changes to a dingy flesh color and then to black or blackish where wounded, as in the type. Castanea dentata ( Marsh.) Borkh, There is a chestnut tree near Freehold, Greene co., in which the ‘nvolucre of the fruit is rudimentary or abortive. It consists of a mere shallow cup or rim which surrounds the base of the fruit. The tree is known to the inhabitants of the place as the burless chestnut. It blossomed freely the past summer but failed to develop _ fruit. It is said that the boys are so eager for the nuts that the owner of the tree realizes but small returns from it. As it is the only tree of its kind known to us it would seem desirable that it should be perpetuated either by planting its seeds or grafting scions of it on other chestnut trees. Catastoma circumscissum (B. & C.) Morg. This curious little puffball which ruptures at the base when mature, as indicated by the generic name, is more plentiful in more western regions. It has been found in two localities in our State, one in St Lawrence county, the other in Essex county. Chrysomyxa pyrolae (DC.) Rostr. As indicated by the specific name, this species usually inhabits the living leaves of various kinds of Pyrola, but the uredo spores were discovered the past season near Friends lake, inhabiting living leaves’ of Momeses, umitlora: (Da Gray ae imine Clavaria bicolor Pk. This name, being antedated by Clavaria bicolor Mass was changed in Sy\lloge 17, page 196 to Clavaria peckii Sace & D. Sacc. This name having previously been used in Sylloge 9, page 249, was not available in this case. Therefore the name Clavaria vestitipes is here substituted for Clavatim bicolor in N. Y. State Museum bulletin 54, page.954. Craterellus cantharellus (Schw.) Fr. A form of this mushroom occurred plentifully the past season neat Menands. The hymenium was distinctly marked by branched and anastomosing folds or narrow blunt edged lamellae, so that the plants might easily be mistaken for the common yellow, chantarelle. 5 REPORT OF THE STATE BOTANIST 1906 35 In the dried specimens the folds have disappeared from the hymenium near the stem but they are very distinct toward the margin. In other respects these mushrooms maintain the characters of the species. We propose for them the name Craterellus €Cantharellus intermedius n. var. - The hymenium is in- termediate in character between that of Cantharellus and Craterellus, Dryopteris simulata Dav. Fine specimens of this delicate fernewere found near “ Merrell Avenue,” Richmond co. by Mr P. Dowell and contributed by him to the State herbarium. Eleocharis intermedia habereri Fern. Sandy shore of Oneida lake at Lewis point, Madison co. August. J. V. Haberer. In this variety the bristles are rudimentary or en- tirely wanting. Fusarium sclerodermatis Pk. This name is antedated by Fusarium sclerodermatis Oud. The New York fungus has the same habitat as the other and is so closely related to it that, in our opinion, it is only a less fully developed form of it. Inocybe calamistrata Fr. A form of this species sometimes occurs in which the usual dingy blue tint at the base of the stem is wanting. Such specimens were collected near Friends lake in July. They were growing with the normal form. Irpex canescens Fr. Fine specimens of this species were found in woods near Wading River. ‘They were growing on dead branches of an apple tree, and developed on the underside of the branches. On branches less than an inch thick, a free margin projected 3 or 4 lines on each side. The hymenium of these margins had the appearance of the hymenium of some Lenzites, the plates being lamellalike and running at right angles to the axis of the branch and parallel to each other, occasion- ally branching or anastomosing. Lactarius pergamenus Fr. This mushroom seems to intergrade with Lactarius piper- atus Fr. Specimens sometimes occur that might with almost equal propriety be referred to either species. But specimens were found 36 NEW YORK STATE MUSEUM near Wading River in which the prominent distinguishing charac- ters of the species were so well expressed that the identity of the species could be easily recognized. The thin, narrow and very crowded lamellae and the thin and flexible pileus were satisfactorily shown. — Lobelia dortmanna L. In Gray’s Manual the water lobelia is described as being 5-12 inches high; in Britton and Brown’s Illustrated Flora, 6-18 inches. Specimens of this plant were collected in Friends lake that are 30-35 inches tall. They grew in deep water which is evidently one factor in determining the length of the stem. Lycoperdon pedicellatum Pk. On account of the permanently pedicellate spores of this very distinct puffball the species has been transferred from the genus Lycoperdon to Bovistella and bears the name Bovistella pedicellatum (Pk.) Lloyd. Panus fulvidus Bres. So far as can be ascertained from the descriptions of this species of mushroom and Lentinus sulcatus Berk. they are specific- ally the same. The uneven or denticulate edge of the lamellae of L. sulcatus is not mentioned in the description of P. fulvig dus, but in the other characters there appears to be complete agreement. The specimens which in State Museum bulletin 105, page 26 are referred to P. fulvidus have the eroded or den- ticulate edge of the lamellae ascribed to Lentinus sulcatus. and as this species antedates Panus f ulvidus our specimens should take the name Lentinus sulcatus Berk. This species was founded on specimens collected in Ohio. Paxillus panuoides Fr. A singular form of this species was found at Glens Falls by. Dr H. von Schrenk growing on pulp paper that had been stored for a considerable time in an inclosure where there was not much light. Both habitat and place were unusual and evidently had a modifying ‘nfluence on the character of the specimens. Some of them were 4 inches long, including the narrowed stemlike base, and 2 or 3 inches broad. They were nearly white when fresh but in drying — they gradually assumed a yellowish tint approaching the normal REPORT OF THE STATE BOTANIST 1906 37° color of the species. Smaller specimens were found growing near these but in a more exposed place. These had the usual color of the species. Peziza (Mollisia) typhae Pk. This name is antedated by Peziza (Mollisia) typhae Cke. Though bearing the same name the two fungi appear to be quite distinct. In the New York species the cups are superficial and the disk is much paler than in the other and the spores are much smaller. We therefore substitute the name Mollisia palli- dior for Peziza (Mollisia) typhae Pk. in New York State Museum Report 32, page 47. Physarum lateritium (B. & R.) Rost. Bark in woods. Lyndonville, Orleans. co. Autumn. Scarce. C.E. Fairman. The Lyndonville specimens differ from the typical form in having the lime granules of the peridium and the nodules of the capillitium yellow instead of red. _ Polystichum acrostichoides incisum (Gr.) Under. Pound Ridge, Westchester co. July. Mrs E. S. Tomlinson The specimen is a very broad one, the frond being nearly 6 inches broad in its widest part. The fruiting pinnae are not abruptly re- duced in size as in the ordinary form of the species. Populus balsamifera L. In the town of Sand Lake, Rensselaer co. there is an outlying and unusually southern station of this northern tree, the balsam poplar. The trees are few in number but they have existed there for many years. Those bearing pistillate aments predominate, but staminate aments are borne by at least one tree. The location is so far south of the general range of the species that late frosts often kill the early starting blossoms and prevent the development of fruit. Some- times when this does not occur the crop of pollen seems to be in- sufficient for the general pollination of the pistillate blossoms. Last spring many pistillate aments were found with only three or four fruit pods developed, the others having prematurely fallen. The lack of proper pollination was probably the cause. The leaves on the older and less vigorous branches are somewhat thomboidal and pointed at both ends, but those on young and vigor- ous branches are more ovate and broadly rounded or even truncate at the base. Both kinds of leaves grow on different branches of 38 ' NEW YORK STATE MUSEUM the same tree. The species is northern in its range and is common ~ in the Adirondack region. Crevices of walls and pavements. Utica.” September. This is — an unusual location for the procumbent pearlwort. Its occurrence ~ here was made known to me by Dr Haberer. It forms rather dense ~ compact mats. In Paine’s Catalogue of Oneida County Plants its — habitat is given as “ wet sandy banks and shores.” It is recorded — as “rare”’ but no definite station is mentioned. f Sagina procumbens L. ; é | : Scirpus atrovirens pycnocephalus Fern. Shore of Oneida lake at Lewis point, Madison co. August. Scirpus cyperinus pelius Fern. Open woods 3 miles south of Utica. August. J. V. Habererag Near Hranktort, Flerkimer co. ) September. @s la) Peck ‘ Trametes serialis Fr. On pulp paper. Glens Falls. October. H. von Schrenk. Them specimens are white throughout and therefore the growth of the present season. The usual habitat in the Adirondack region is dead wood of spruce. Trillium erectum album Pursh : Near Syracuse. May. Mrs L. L. Goodrich. In the contributed — specimen the petals are yellowish. This form has been unusually — plentiful this year and might easily be considered as good a variety — as the form with white petals. Viola cucullata Ait. A peculiar form of this species occurs in North Greenbush. In. it the scapes are about as long as the leaves, the tips of the petals are white or whitish and also the basal angles of some of the leaves. EDIBLE FUNGI Tricholoma hirtellum n. sp. HAIRY CAP TRICHOLOMA PLATE 105, FIG. I-5 ; Pileus fleshy, thin, convex, subumbonate, dry, hairy, pale brown, flesh white, taste mild; lamellae thin, narrow, close, slightly sinuate, ‘ REPORT OF THE STATE BOTANIST 1906 39 adnexed, minutely floccose on the edge, yellowish white or pallid; stem slender, equal, stuffed or hollow, with a very small cavity, fibrillose or subsquamulose, colored like or a little paler than the pileus ; spores subglobose, .00024—.0003 of an inch long, .0002—.00024 broad. The hairy cap tricholoma grows in tufts or singly on or about pine stumps in Wading River, Suffolk co. and occurs in August. It is a very rare species and has been found but once. It is related to Tricholoma albofimbriatum Trog., from which it is separated by its hairy cap, white flesh and less crowded gills not fimbriate on the margin. The hairs of the cap are often collected in minute tufts giving the cap an appearance similar to that of the brownish caps of the honey-colored armillaria, but unlike that _ species it never has a collar on the stem. The caps are 1-1.5 inches broad, the stem 2-3 inches long and 2-3 lines thick. Tricholoma nudum (Bull.) Fr. NAKED TRICHOLOMA TILVANINIS, OL, IBCs | 10) Pileus thin, broadly convex, nearly plane or slightly depressed in the center, obtuse or occasionally slightly umbofate, incurved on the thin naked margin when young, pale violaceous or lavender, fading with age and the escape of moisture to a pale grayish brown, often slightly tinged with reddish or yellowish hues, flesh of the young plant tinged with the color of the pileus, becoming white with age, taste mild; lamellae thin, narrow, close, slightly sinuate, adnate or decurrent, colored like the pileus when young, becoming whitish with age; stem firm, equal, fibrous, stuffed or hollow, colored like ‘the piieus; spores pale flesh color in mass, elliptic, .00024—.0003 of an inch long, .0o012—.00016 broad. The naked tricholoma is a rare species with us. The specimens tested and figured on plate 104 were collected in Electric park, Columbia co., October 29, by Mr S. H. Burnham. The plants were found growing in flower beds, either singly or in clusters, and when young and fresh they are throughout of a beautiful violet color ap- proaching lavender, but this color fades and changes with age and with the escape of moisture and the cap becomes a pale pinkish gray or dingy reddish, the stem and gills also changing in a similar man- ner. ‘The cap is generally obtuse but sometimes umbonate. The “Margin is very thin and when young is incurved and sometimes 40 NEW YORK STATE MUSEUM striatulate, the obscure striations being the shadowy lines of the gills showing through the membranous and almost translucent sub- stance of the margin. In drying, the excessive moisture escapes from the center of the cap first. The margin is naked even in young plants and in this character the species differs from its near relative, the masked tricholoma. It is also smaller than that species and more highly colored when young. The naked margin is probably the character which suggested the name of the species. The typical form of the species is described as having a stuffed stem. In our plants the stem is sometimes clearly hollow. An acid odor has been ascribed to the species but no distinct odor was perceptible in our specimens. European mycologists do not appear to have given very definitely the color of the spores of this species. Professor Fries describes the spores of the species referred by him to Paxillus, tribe. Lepista, as sordid, and W. G. Smith, who raised this tribe to generic rank and referred both Tricholoma nudum and T. per- sonatum to it, says the spores are dirty white. In our plant the spores are pale flesh color and indicate a close relationship between this species and those of the pink spored series, specially those in the genus Clitopilus. But the close connection between this species and Tricholoma personatum persuades us at present to let the species remain where it has so long stood not- withstanding the peculiar spore color. The cap in our specimens is I-3 inches broad, the stem 1-2 inches Jong and 2-4 lines thick. Stevenson says of the European plant, “ Not recommended as edible.” Gillet says “very good” and “very delicate” but rarely used. In our trial of it we found it agreeable in flavor, digestible and harmless and have no hesitation in placing it among the edible species. Its worst defect is its scarcity. Clitocybe amethystina (Bolt.) LIMO RIN SNES Ih (CL IMlOXE WABI 8. PLATE 100, FIG. I-6 Pileus at first hemispheric, becoming broadly convex or nearly plane, hygrophanous, often. obscurely striate on the margin when | young and moist, depressed in the center or frequently umbilicate, often irregular, violaceous when moist, grayish or grayish white when dry; lamellae rather thick, subdistant, violaceous, adnate or slightly decurrent; stem slender, rigid, straight or flexuose, stuffed, REPORT OF THE STATE BOTANIST 1900 4!I becoming hollow, paler than the moist pileus; spores globose, verru- cose, .0003-.0004 of an inch broad. The amethyst elitocybe is a small species, gregarious in its mode of growth and slightly tough. European mycologists have gener- ally considered it as a mere form or at most a variety of Clito- cybe laccata (Scop.) Fr. Berkeley and Broome instituted a new genus, Laccaria, for the reception of C. laccata and allied species with tough substance, hymenophorum confluent with the stem, and thick gills powdered with white globose spores. They re- mark that the amethyst colored form usually referred to Agari- cus laccatus is probably distinct. Their genus has not yet been generally accepted but there is good ground for its establishment and it probably will be recognized in due time. Their remark con- cerning the amethyst colored form of C. laccata appears to us to be worthy of acceptance and it is therefore accepted here as a distinct species. It is easily recognizable both in its fresh and dried state from the paler and more common form usually referred to C.laccata. It is very constant in its characters and no inter- mediate forms occur to connect them. It is quite as good as an edible mushroom. In drying, the gills retain their violaceous color longer than the cap. - _ Clitocybe ochropurpurea Berk. PUR PLISHVOCHER: CLIMOCYBE PLATE 100, FIG. 7—-II Pileus subhemispheric, becoming convex with a decurved margin or nearly plane and slightly centrally depressed, fleshy, tough, com- pact, hygrophanous, purplish brown when moist, grayish or pale alutaceous when dry, unpolished; lamellae thick, distant, broad, narrower outwardly, adnate or decurrent, purple; stem variable, short or long, equal, or sometimes thicker in the middle, sometimes at each end, fibrous, solid, colored like or paler than the pileus; spores globose, white, verrucose, .0003-.0004 of an inch broad. The purplish ocher clitocybe is related to such species as the laccate clitocybe, C.laccata, and the amethyst’ clitocybe, C. amethystina. From both it is easily separated by its purple gills and larger size. It is found in wet weather from July to September. It grows in open grassy places and is sometimes quite irregular in shape. Its cap is often 3-4 inches broad and its 42 NEW YORK STATE MUSEUM stem 4-6 lines thick. As an edible species it is rather tough but its flavor is agreeable if well cooked and seasoned and it is harmless, Should the proposed genus Laccaria be recognized the name of the present species would be Laccaria ochropurpumed (Berk.) and that of the preceding species would be Laccaria’ amethystina (Bolt.) Cke. Russula compacta Frost COMPACITRUSSUIEA PLATE 100, FIG. I-4 Pileus fleshy, compact, broadly convex, becoming centrally de- pressed or infundibuliform by the elevation of the margin, dry or slightly viscid after rain, unpolished, at first whitish slightly clouded with reddish buff, or rusty red with whitish margin, becoming en- tirely rusty red with age, flesh white, taste mild or slightly and tardily acrid; lamellae close, adnate or slightly rounded behind, unequal, some forked, white, changing to reddish brown where wounded and in drying; stem short, stout, firm, solid or sometimes cavernous, white, becoming stained where bruised; spores white, globose or subglobose, .0003-.00035 of an inch broad. The compact russula is a large mushroom belonging to the Friesian section Compactae. It is allied to the European Russula mustelina Fr. from which it may be separated by its different color, which changes with age, and by its disagreeable odor in dry- ing. The cap is usually 2-4 inches broad, but sometimes it attains a diameter of 6 inches. Its stem is short, equal, stout and firm, white when young but usually becoming colored like the cap. It is 2-2.5 inches long, 8-18 lines thick. It furnishes an abundance of agreeable food, the flesh being so thick and compact. Russula earlei Pk. EARLE RUSSULA State Mus. Bul. 67, p. 24, pl. N, fig. 5-10. The Earle russula is a very distinct and easily recognized species. No one of our other species has such distant gills combined with such small white spores. These characters in connection with its very viscid or glutinous and pale yellow or straw colored cap make it scarcely possible to confuse it with any other species. It has hitherto been found on Long Island only. It occurs in August. , F REPORT OF THE STATE BOTANIST 1906 43 Russula pectinatoides n. sp. 2S CAINS, PAWSON PLATE 105, FIG. 6-10 Pileus thin, broadly convex becoming nearly plane or centrally depressed, viscid when moist, widely tuberculose striate on the margin, brownish or yellowish brown, sometimes darker in the center, flesh white, grayish white under the separable cuticle, taste mild or slightly acrid; lamellae thin, a few forked at the base, occa- sionally a short one, adnate, white becoming pallid; stem equal, spongy within, even, glabrous, white; spores whitish, subglobose, .00025~.0003 of an inch long. , Grassy ground in groves or pastures. The pectenlike russula is pamilar to Russula pectinata (Bull.) Fr. from which it differs in its mild or slightly acrid flavor, its even stem, in its flesh being grayish white under the cuticle and in its adnate gills. It is gregarious or scattered in its mode of growth and is not plentiful. It closely resembles Russula sororia Fr. in its general ap- pearance, but may be separated from it by its milder taste. Its cap is 1-3 inches broad; its stem is 1-2 inches long and 3-4 lines thick. It appears in July and August. It is edible but not very highly flavored. Russula uncialis Pk. INCH WIDE RUSSULA PLATE 107, FIG. 7-12 Pileus thin, convex becoming expanded or centrally depressed, viscid when moist, glabrous or very minutely rivulose-granulose, red or pinkish red, the margin obscurely tuberculose striate, flesh white, taste mild; lamellae moderately close, narrowed toward the stem at which a few of them in some specimens are forked, adnate or slightly emarginate, white, the interspaces venose; stem equal, glabrous stuffed or spongy within, white or reddish; spores white, globose, rough, .0003—.00035 of an inch in diameter. The inch wide russula belongs to the subgenus Fragiles, white spore group. It is about as large as Russula fragilis, but may be distinguished from it by its mild taste and less crowded gills. From similarly colored specimens of R.chameleontina it differs in its white spores and gills. The gills become pallid in drying. 44 NEW YORK STATE MUSEUM Agaricus micromegethus Pk. SMALL MUSHROOM PLATE 107, FIG. 1-6 Aearreus pusillas Rk NY) States Muse Repits Aap nse: Pileus fleshy but thin, fragile, convex, becoming plane, sometimes slightly depressed in the center, dry, silky fibrillose or fibrillose- squamulose, grayish brown, darker or brown in the center, often with yellowish or ferruginous stains, flesh white or whitish, not changing color where wounded, taste and.odor almond; lamellae thin, close, free, grayish, soon pinkish, finally brown; stem equal or slightly tapering upward, sometimes bulbous, stuffed or hollow, slightly fibrillose, white, the annulus slight, often evanescent; spores broadly elliptic or subglobose, .ooo2 of an inch long, .00016 broad. The specimens from which this species was first described were smaller than others collected later. The caps in these now before us are I-3 inches broad and the stems 1-2 inches long and 3-5 lines thick. The flesh is white and unchangeable when cut or wounded. It has a taste resembling that of almonds which has given origin to the local name “almond mushroom.” One correspondent says that “it is the finest flavored mushroom he has ever tasted.’ Bruises of the cap and stem of the fresh plant sometimes assume a yellow color. The plants grow singly or in clusters. They appear from September to November, and have been found growing in both sandy and clayey soil, and in tan yards. The range is from Michi- gan to Massachusetts. Boletus frostii Russell ~ FROST BOLETUS PLATE 108, FIG. I-5 Pileus convex, firm when young, becoming softer with age, gla- brous, viscid, dark red becoming paler with age, flesh whitish, tinged with yellow next the tubes, taste slightly acrid; tubes concave in the young plant, becoming plane or convex, adnate, yellowish with their mouths colored like the pileus, changing to bluish green where — wounded ; stem equal or nearly so, solid, strongly reticulate, colored like the pileus, yellow within, often with reddish stains at the base; spores with a greenish hue when caught on white paper, subfusiform, .0005-.0006 of an inch long, .0002 broad. The frost boletus is a very showy species. Its deep red cap and — distinctly reticulate red stem are attractive to the eyes and a delight _ REPORT OF THE STATE BOTANIST 1906 45 to the mycologist. It occurs in our State on Long Island and so far as known is not found elsewhere within our limits. Its viscid cap is 2-4 inches broad and its stem about as long and 4-6 lines thick. It grows both in thin woods and in open places and occurs during July and August. According to the old rule, which pro- nounced all species of which the broken flesh assumed a blue color to be unfit for food and dangerous, this species should be rejected. But this rule must have its exceptions. I have eaten of this boletus without harm and one of my correspondents writes that he has | eaten four caps of it at a meal and considers it an excellent species. Boletus rugosiceps Pk. RUGOSE CAP BOLETUS State Mus. Bul. 94, p. 20, pl. QO, fig. 6-10. The rugose cap boletus is well marked by its yellowish ochraceous cap which is irregularly uneven by unequal and variously shaped pits or depressions in its surface. It is sometimes slightly tinged with red or orange and occasionally embellished with small areolae formed by cracks in the surface. The surface is viscid and shining when moist and the flesh is white or whitish. The tubes are at first closed but they soon open, are minute, round and yellow, becoming darker with age. The stem is solid and firm in texture, often marked with elevated longitudinal lines or ridges and dotted with numerous points which are variable in color, being either pallid, brownish or yellowish. The cap is 1-3 inches broad, the stem 2-4 inches long and 4-8 lines thick. The plants grow in thin woods and may be found in August. They have been found on Long Island but not in other parts of the State. In preparing them for the table it is well to peel away the cuticle and the tubes and discard the stem. NEW YORK SPECIES OF HYGROPHORUS Hygrophorus Fr. Hymenophorum continuous with the stem, descending unchanged into the trama; lamellae acute on the edge, clothed with a hymenium changeable into a waxy mass, not membranaceous; spores globose elliptic or ovoid, white. Terrestrial putrescent fungi with a viscid or moist pileus. The waxy character of the hymenium is the chief distinguishing character of the genus. The lamellae are usually thick, distant or subdistant, and their hymenial surfaces somewhat separable from 46 NEW YORK STATE MUSEUM the trama. Many species with decurrent gills are similar in appear- ance to species of Clitocybe, but such species may generally be dis- tinguished by their distant lamellae and their viscid pileus and stem. The genus was divided by Fries into three tribes or subgenera which have not yet been accepted as genera but they probably will be in due time. The foliowing synoptic key indicates the prominent characters that may be employed in their separation. KEY TO THE SUBGENERA Stem solid: or. stutted). 24) 2.0. eae. nee oe eee eee I Stent hollow .c2.004- See toe hoes scars. ene ote hoe Bee Hygrocybe in SEMIS) TOMONME IMO WICIGle sn aosoocnbuscenocdseodeococee ,...Camarophyllus t-Piléus and stem viscid<-ck. setae eos ee eee eee Limacium Limacium Fr. Universal veil viscid with a partial floccose veil sometimes forming a ring or attached to the margin of the pileus; lamellae adnate or decurrent; stem clothed with squamules or more often scabrous punctate at the top (or sometimes glabrous). In this subgenus the pileus and stem are normally viscid but in Hygrophorus purpurascens Fr. and Hy eapmeoies rius Kalchb. they soon become dry. The stem is usually solid or stuffed, but in H. eburneus Fr. and Hy hy potmejme Fr. it often becomes hollow. H. pudorinus Fr. is described as having no veil, but the pileus and stem are viscid. Perhaps the “velum nullum” has reference to the partial floccose veil only. There are several species in which the stem is neither squamulose nor scabrous punctate at the top. In other respects they agree with the description of this subgenus. They are H. fuligin- eus- Frost, H. ftlavodiscus Prost, EH. specvosu ome HW. subviolaceus Pk, H. hypothejus Mr anda lividoalbus Fr. This might justify the formation of a new © subgenus for their reception, but since Fries himself has placed several similar European species in his subgenus Limacium, thus practically recogpizing this additional character, it has seemed better to extend the characters of the subgenus, as Fries has done in fact though not in words, than to found another subgenus on such a slight difference. KEY TO THE SPECIES Pileus white, or white with the center yellowish or brownish......... I Pileus pinkish, violaceous or red or purple with paler margin........... 7 Pileus..livid “white; cineneous or browne teeee ss. oe Ul 1 Margin of pileus with yellow floccose points.................. chrysodon © & Margin of ‘the piledstnaked:., 8.02044. oe eee 2 REPORT OF THE STATE BOTANIST 1906 47 PRS Seti Ol Oye WiletI MIVAULLITE > 43, qercbo 5 cence tye areas, ok els ks bun akne eo 3 Pestem solid or stuited, not hollow when mature......0.............. A eI CMU eee Racy ea mir eis Gets mre es linn o's astecc oom sain & see « eburneus Peenmeliaensyellow cor, yellowishe so. 5s. 264 esc saves ons ose ae hypothejus 4 Lamellae becoming brownish with age or in drying..... Pentel sbin iichaoe 5 Peecmcliae persistently white Of whitish. *.-...0......022...+s5.4e0:- 6 meeiiets slichtly virgate with innate fibrils.....:.............0... virgatulus SeMISMNTOU NI TULOSE! ain cist fc cates «tate Sate ace aa ee ee ee 6 ‘ REPORT OF THE STATE BOTANIST 19006 59 sh seisrenGl wrest SE eerie WE Ra a eee anes fete ee on ey ate 10 PEC MSO Ia er Sh GiaOMt REC sis. oe ats een ce Gime atic aes tisteeieewars shades « 7 & IPCC TONE ene el U | a esa me Bees Bereich eth NOM eae eRe ce ceraceus Seensme Tavis redvon Tawi hed: oancuc saws cts dosSwe aero dn esis laricinus Megemtenpe ted. Orange Of SCablets..:. 1. ens ved seen Grentias weedaaee 8 S IPulle@ws - AS MIREliie CovaiKC eee Gee Gornvaters once nna cic Ole ot tien eee conicus SMe SpenOt ma cubely INC@mMIGwae, piacere aya Rites negate woe Wee ovules a 9 MEEETDMECE WL ads Wihte: DASCY «ves ce 52 ajc etree wn Sev eed a ees weet puniceus SePBtnmEcCnwitiaeyellOw= DAS@i..cccce- se easeoe vee gen cae oe enw coccineus 10 Stem and pileus with greenish slime when young................. II ROMSLEMMANGs plleus mot, ereenishe wi. wslsusoaeuoneoscacs yeceanmeen. 12 MPMI CACC is Clits me aes ata are ato eens SUR Athans cesses mylopereee ole cudnt os peckii 2 TLavamellilee: iG hivehicins, Bec cyssne enero eer CaenCio ike Rea Lee Cree i eae ree psittacinus TD TE AT eeis MSS es Geese to eter ee cae ic a purus 1D JPulleweesy TRON eatery gem cia ous AoC MNO Ie eacie PEER Ree an rarer eee ipa luridus BemiMeis meiticn white MOT PFOWM)... 02. 2.0.6 cee ema nese ne sie ne eee wl 13 Reemeomlessy tian) 6) lines Proad... seus o octet ane eee laeel ass cdes minutulus Beevensemore: than © Lines, broad) 4s 0c .c ccs s deen scieies 6 vee dba cen cele. 14 iat [Phillis -aniral bp Ce Nea Y Sas areecs ce oreo Riccieare Tn Pekar nitidus BD een Mer OL aU CALC Ay evs anit oe sich enn aye cee Meafeon.cuaid Sierg ek 6 6 by arene 15 + lLamnellag fevalinnesrceyalls Sis errciy: ccanch aor a cr a ao ecnee ecw ici ren Pecan einen chlorophanus Bee ictidtcmadnatenor Cecunrent