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NIN 7% : 7, New York State Education Department NEW YORK STATE MUSEUM 63d ANNUAL REPORT ee In 4 volumes VOLUME 1 REPORT OF THE DIRECTOR 1909 AND APPENDIX I Kou \ INS TIS | ON SEP 2 PO Fo ie ~_V E yw Yo SATIONAL MUSESE TRANSMITTED TO THE LEGISLATURE FEBRUARY a1 21, 1O1O ALBANY UNIVERSITY OF THE STATE OF NEW YORK Igit STATE“OF NEW YORK EDUCATION DEPARTMENT Regents of the University With years when terms expire 1913 WHITELAW Reip M.A. LL.D. D.C.L. Chancellor New York 1917 ST CLainR McKetway M.A. LL.D. Vice Chancellor Brooklyn 191g DanieL BEacH Ph.D. LL.D. - - - - - Watkins 1914 Puiny T. Sexton LL.B. LL.D. -—.- -— -— -— Palmyra 1912 T. GuiItForp SmiTH M.A. C.E. LL.D. - — .- Buffalo 1918 Witt1am Nottincuam M.A. Ph.D. LL.D. - - Syracuse 1922 CHESTER S. Lorp M.A. LL.D. - - - —- - New York 1915 ALBERT VANDER VEER M.D. M.A. Ph.D. LL.D. Albany 1911 EpDwarRD LAUTERBACH M.A. LL.D. - - -— -— New York 1920 EuGENE A. Puitpin LL.B. LL.D. - - - - New York 1916 Lucian L. SHEDDEN LL.B. LL.D. - - - - Plattsburg 1921 Francis M. CARPENTER - - - - - -— -— Mount Kisco Commissioner of Education ANDREW S. DRAPER LL.B. LL.D. Assistant Commissioners Avucustus S. Downinec M.A. Pd.D. LL.D. First Assistant CuHar_es F. WHEELOCK B.S. LL.D. Second Assistant Tuomas E. FineGan M.A. Pd.D. Third Assistant Director of State Library James I. Wyer, Jr, M.L.S. Director of Science and State Museum Joun M. Crarxke Ph.D. D.Sc. LL.D. Chiefs of Divisions Administration, GEorcE M. Witzy M.A. Attendance, JaMEs D. SULLIVAN Educational Extension, WILLIAM R. EastmMAN M A MLS. Examinations, HARLAN H. Horner B.A. Inspections, FRanK H. Woop M.A. Law, FRANK B. GILBERT B.A. School Libraries, CHARLES E. Fitcu L.H.D. Statistics, Hiram C. CasE Trades Schools, ARTHUR D. DEAN B.S. Visual Instruction, ALFRED W. Asrams Ph.B. eee. | oO -NZAT2 | | PratrE OF New YorK —— No. 45 IN ASSEMBLY FEBRUARY 21, I910 63d ANNUAL REPORT OF THE NEW YORK STATE MUSEUM VOLUME 1 To the Legislature of the State of New York We have the honor to submit herewith, pursuant to law, as the 63d Annual Report of the New York State Museum, the report of the Director, including the reports of the State Geologist and State Paleontologist, and the reports of the. State Entomologist and the State Botanist, with appendixes. St Cratrr McKELway Vice Chancellor of the Umversity ANDREW S. DRAPER Commussioner of Education CONTENTS VOLUME 1 Report of the Director 1909 PAGE e PAGE Symmetric Arrangement in the Tatroduetion ats curse Secu, Na ee aS Ae Gente Of hen. Daleonoin I Condition of the scientific col- Platformmof North Aameren eCtONSs Wa teeta bo Bosc Rupotr RUEDEMANN......... TAI II Report on the geological sur- ViEV iE oie a tetrn colors ce kebetedehans ‘ees atiey at 8 Origin of Color in the Vernon Geological survey ...-.-...... 8 7 ae Shales | Wie lee MULE eRe wei ~ 150 Seismological station <2 .4: 5. «. 35 Mineralogy Been Bala Pacharealese mul er 39 | Downward Overthrust Fault at Paleontology.) yacee. ces lea 40 Satigerties),” IN Ye pc Gaaeele III Report of the State Botanist.47 CHADWICK ..........+...45. 057 IV Report of the State Ento- Joint Caves of Valcour Island — MOLORISE +. o« < ge eh See vo 48 Their Age and Their Origin. ; V Report on the zoology section 54} ™§ G. H. ELGpsON (eee 161 TR h h pele . VE Regert on the archeslogy- | céntthitfons to. Mineral Wit seablicationsys 2) 20s] semen 69 HP. WE hoee 2a cu NIM State tee certo tle. a eee 75 | The Iroquois and the Struggle CSAC CERCTOTISn to. cee ines no 96 [eres for America. ELtHu Root. .204 Age and Relations of the Little Nun-da-wa’-o, the Oldest Seneca Falls Dolomite (Calciferous) «9 Village: D. DP Wormers ene of the Mohawk Valley. E. O. ! UrricH Gey alte ee CUSHING 97 ‘Index erate pina cit fea eeet nese sag Appendix I ‘i A Museum Bulletins 135, 1373 Ree I Geology 135 Geology of the Port Leyden. Quadrangle, Lewis County, N. Y. W. J. MILrtER 137. Geology of the Auburn-Genoa Quadrangles. D. D. LUTHER © 138 Geology of the Elizabethtown and Port oe Quadrangles James F. Kemp and RupoLF RUEDEMANN VOLUME 2 Appendixes 2-4 Museum Bulletins 142, 143, 136, 141, 139 2 Economic seology 142 ‘The Mining and Quarry. Industry of New York State 1909. Dire NEWLAND 143 Gypsum Deposits of New York. D. H. NEw Lanp “&” HENRY LEIGHTON 3. Entomology 126 Control of Flies and” Other Houconaler Ince ee EPs baer 141 25th Report of the State Entomologist-19090. E. P.-FEerr © ~~ 4 Botany 139 Report of the State Botanist 1909. C. H. Peck VOLUME 3 ' Appendix 5 Museum Memoir 12, part 1 Birds of New York. E. H. Eaton VOLUME 4 Appendix 6 Museum Memoir'13 Calcites of New York. H. P. WuHItTLocK Education Department Bulletin Published fortnightly by the University of the State of New York Entered as second-class matter June 24, 1908, at the Post Office at Albany, N. Y., under the act of July 16, 1894 No. 473 SE TEAGN Ys ND ONG JUNE 52.2016 New York State Museum Joun M. CriarKeE, Director Museum Bulletin 140 SIXTH REPORT OF THE DIRECTOR OF THE SCIENCE DIVISION INCLUDING THE 63D REPORT OF THE STATE MUSEUM, THE 29th REPORT OF THE STATE GEOLOGIST, AND THE REPORT OF THE STATE PALEONTOLOGIST FOR 1909 PAGE PAGE BaP RMU MEMOM. ) su wc es 5 | symmetric Arrangement in the I Condition of the scientific col- Elements of the Paleozoic TOES Wen oes ose Ss 6 Platform of North America. II Report on the geological sur- UO ISB IPUES Go oo ae SERMONS ce a ne eas. G-Soo a 8 | Origin of Color in the Vernon Geolorical survey :..:,.-... 8 Sales Wee). MImluimRe 2. ...150 peismolovical station........ a pees een ea a Downward Overthrust Fault at Pee OMLOIODY 01... sse 2. ee ~=40 peecnee NE Gag di. III Report of the State Botanist 47 crt thie” Sa cre canis ae 157 IV Report of the State Ento- Joint Caves of Valcour Island— MET HN Sh aks Sake tsa 3 os 48 Their Age and Their Origin. V Report on the zoology section 54 Galina WIS ONE moar ine ss 161 VIR t th cheol Poo .............. 59 | Contributions to Mineralogy. Reeeeewiieations . 2.5... ..6.... 69 oe 197 SPP yi sey hs Saks 75 | The Iroquois and the Struggle MemereeecSNOUS. i) 0.05. we 76 for America. Erinu Root 204 Age and Relations of the Little Nun-da-wa’-o, the Oldest Seneca Falls Dolomite (Calciferous) Village. D.D. Luruer....213 of the Mohawk Valley. E.O. emeLemerLtF CUSHING oF | Indéye seo... cl ks. 22% i ene Fae at © Pal ieee ~- eS ee ee Se rr FO. New York State Education Department Science Division, February 15, 1910 Fon. Andrew S. Draper LL.D. Commissioner of Education Sir: I communicate to you herewith for publication as a bul- letin of the State Museum, the Sixth Annual Report of the Director of the Science Division for the fiscal year ending September 30, 1909. ‘Very respectfully JoHN M. CLARKE Director State of New York Education Department COMMISSIONER’S ROOM Approved for publication this 21st day of February I9f0 Commissioner of Education Education Department Bulletin Published fortnightly by the University of the State of New York Entered as second-class matter dune 24, 1908, at the Post Office at Albany, N. Y., under he act of July 16, 1894 No. 473 ALBANY, N. Y. JUNE 15, 1910 New York State Museum | JouHn M. Crarke, Director Museum Bulletin 140 SIXTH REPORT OF THE DIRECTOR OF THE SCIENCE DIVISION INCLUDING THE foe OoR! OF THE STATE MUSEUM, THE 2oth REPORT OF Peis GEOLOGIST, AND THE REPORT OF THE perv PALEONTOLOGIST FOR 10909 DIRECTOR’S REPORT FOR 10909 INTRODUCTION This report covers all divisions of the scientific work under the charge of the Education Department and concerns the progress made therein during the fiscal year 1g08-9. It constitutes the 63d annual report of the State Museum and is introductory to all the scientific memoirs, bulletins and other publications issued from this office during the year mentioned. Under the action of the Regents of the University (April 26, 1904) the work of the Science Division is “under the immediate supervision of the Commissioner of Education,’ and the advisory committee of the Board of Regents of the University having the affairs of this division in charge are the Honorables: T. Guilford ita.) Buttalo; Daniel Beach LL.D., Watkins; Lucian L. Shedden LL.D., Plattsburg. The subjects to be presented in this report are considered under the following chapters: 6 NEW YORK STATE MUSEUM I Condition of the scientific collections II Report on the Geological Survey, including the work of the State Geologist and Paleontologist, of the Mineralogist, and that in Industrial Geology III Report of the State Botanist IV Report of the State Entomologist. V_ Report on the Zoology section | VI Report on the Archeology section VII Publications of the year VIII Staff of the Science Division and State Museum IX Accessions to the collections X Appendixes (to be continued in subsequent volumes). All the scientific publications of the year if CONDITION OF THE SCIENTIFIC COLLECTIONS 2en— STIUTING THE SPATE MUS mai Since my last report some changes have been necessitated in the location of the collections of the museum, all of which present locations are to be regarded as wholly temporary while awaiting transference to the Education Building. Some displacement from old locations has been necessary to accommodate the demands of the Commissioner of Agriculture for increased room in the Geo- logical Hall. Giving way to these requirements has resulted in again dispersing parts of the collections of the Geological Hall into other buildings in the city of Albany and has involved the De- partment in serious expenditures for rental and maintenance of new quarters. An inevitable disquietude has resulted from these invasions which has been somewhat increased by the preparation necessary for final removal and instalment of all the collections and the progress of new undertakings requiring additional working room. At the present time the collections of the State Museum are dis- tributed as follows: | 1 Geological Hall. In this building there still remain the offices of the Assistant State Geologist and his staff; of the Mineralogist, and some part of the collections in geology, paleontology and mineralogy ; the seismograph is also installed here; also the offices of the State Botanist, with the botanical collections constituting the State her- . SIXTH REPORT OF THE DIRECTOR 1909 7 barium; of the State Entomologist with the collections pertaining _ thereto; of the Zoologist, with all collections in zoology except for instances otherwise specified; workrooms of the taxidermist and archeologist. 2 State Hall. The rooms occupied in this building are the offices of the Director and State Geologist with his immediate staff, together wi:h the extensive collections in paleontology and some others of value. These collections are in drawers and in prepara- tion for removal. 3 Capitol. The corridors of the fourth floor contain on display a very considerable collection in archeology, though only a fraction of such material as is in our custody. In these corridors also are a few cases of mineralogic, paleontologic and ceramic exhibits. On the sixth floor of this building are 100 drawers of minerals and certain large relief maps. In the safe in the Cashier’s office, Education Department are the archives of the Iroquois Nation consisting of wampum belts and other articles of historical importance. 4 McCredie Malthouse. This is the general storehouse for all the collections and equipment of the museum which have been dis- placed by the recent invasions of the Geological Hall or for which no other place can be found. About 500 cases of specimens are here stored. 5 Universalist Church. This building, situated at the corner of Swan and Jay streets, has been rented at the expense of this division and is being utilized as a studio for the artist engaged in prepar- ing the very large background scenery for the Iroquois collection and as office and workroom for the Archeologist. 6 State Normal College. In the corridors of one of the western buildings is temporarily placed, by courtesy of the president, a large, newly mounted group of black bears. eemeperty of j. L. Verstrepen, Delaware street, Albany. Here is a series of large geological specimens which are being removed as opportunity affords. & Flint Granite Company, Cemetery Station. At this place, 3 miles north of Albany, is stored a large and unique slab of trails from the Potsdam sandstone, weighing upward of 20 tons. To this record of 8 widely separated locations in the city of Albany is to be added the fact that there are in storage and under insurance, awaiting transportation whenever accommodations here 8 NEW YORK STATE MUSEUM permit, several large mounted groups of mammals (moose, buffalo and others) in charge of the Ward Natural Science Establishment at Rochester. This much divided and scattered condition of the work is pro- foundly embarrassing and involves serious loss in concentration of effort and of time and enjoins arduous and exacting conditions. Yet it may be regarded as making for progress, as it certainly is now unavoidable in preparing for the equipment of a new museum. This situation has not been allowed to interfere with the progress of the proper scientific investigations of this division, which have taken the direction indicated herewith. II REPORT ON THE GEOLOGICAL SURV EN. VIN@E Ginienis, THE WORK OF THE STATE, GEOLOGiSi a= PALEONTOLOGIST, OF THE MINERALCGE® AND THAT ON INDUSIERTAL GEOROGCy GEOLOGICAL SURVEY Areal geology In the progress of the survey directed toward the execution of the geological map of the State on the topographic scale of 1 mile to 1 inch, a considerable number of topographic quadrangles have been completed and published, with full explanatory details of geological structure. In addition to the completed quadrangles a variety of special maps have been issued in connection with par- ticular geological problems, some of the older of these maps being on such geographic base of approximate accuracy as was best available, but all special maps of later years, whether they have covered limited areas, completed county areas or a series of coun- ties, have been based on the topographic unit. A list of all geologic maps of the State, of every description, was published in my report of last year, and the number was there shown to be large, 329 entries being recorded. I append here a list designed to indicate only the complete quadrangle maps which have been made with special reference to the systematic execution of the State map. In this list the terms starred indicate maps now in press, SIXTH REPORT OF THE DIRECTOR I909 9 *Alexandria Bay (Cushing) Mooers (Woodworth) Amsterdam (Prosser & Cum- Naples (Clarke & Luther) ings ) Nunda (Clarke & Luther) Auburn (Luther) Olean (Glenn) Buffalo (Luther) Ontario Beach (Hartnagel) Canandaigua (Clarke & Luther) Ovid (Luther) *Cape Vincent (Ruedemann) Oyster Bay (Woodworth) *Clayton (Cushing & Ruedemann) Penn Yan (Luther) *Elizabethtown (Kemp) Portage (Clarke & Luther) Elmira (Clarke & Luther) *Port Henry (Kemp & Ruedemann) Genoa (Luther) Port Leyden (Miller) *Grindstone Island (Cushing & Remsen (Miller) Smyth) Rochester (Hartnagel) Hammondsport (Luther) Salamanca (Glenn) Hempstead (Woodworth) *Theresa (Cushing & Ruedemann) Little Falls (Cushing) Tully (Luther) Long Lake (Cushing) Watkins (Clarke & Luther) In addition to these, reports have been rendered to the Director on the quadrangles listed below, these awaiting publication chiefly for completion in certain details. Cazenovia Morrisville Chittenango Syracuse Central and western New York. In western New York final resurvey has been made by Mr Luther of the Caledonia, Honeoye, Wayland and Phelps quadrangles and preliminary control of the Batavia, Attica and Depew quadrangles with an expansion of opera- tions of previous years on the Albion, Medina and Lockport re- gions. These results represent in part the gradual summation of work extending over several seasons and the progressive attack on new fields. In central New York the Utica quadrangle was covered in a preliminary control by Mr Clark and work on the Sangerfield quadrangle progressed by Mr Whitnall. Eastern New York, Saratoga county. Saratoga Springs has, for several years, been the seat of a litigious activity in which the welfare of the mineral water and gas springs is involved, with deep concern to a variety of commercial interests. By virtue of re- cent legislation the State has set itself to save the mineral water springs. It is a worthy but difficult task; worthy, because the Sara- toga springs present a unique geological phenomenon which should be saved from destruction, irrespective of the commercial interests involved; difficult, because the intervention of government has come late and is confronted by large vested rights. ho NEW YORK STATE MUSEUM With regard to the adjudication of important issues now in the courts and arising from the situation at Saratoga, the State Geolo- gist can have nothing to say, but he can and desires to emphasize the fact that the relations of the mineral springs to each other and to the gas springs are a strictly geological problem. These rela- tions must be understood before any determination of intelligent modes of reclamation can be hoped for, and should be compre- hended before any readjustment of recognized rights in the prop- erties involved is attempted. This geological problem is not an easy one. No such problem, deeply buried out of sight and reached only by the drill, is easy. There is probably no place where the subterranean conditions at Saratoga are paralleled and the ob- scurity of their interrelations makes the problem of the source and durability of the waters, their salinity and their pressures one of difficult reach, but the analyses can not be prosecuted by any other mode of attack than the geological. ) The Saratoga springs. have been a fruitful source of theories and vagaries by casual geologists, chemists, mineralogists and hydrog- raphers, which are so frequently contradictory and have been so often exploited, as to weaken confidence in most of the solu- tions proposed. So often have favored contentions for and against one or another exposition of the conditions been promul- gated from the witness stand and elsewhere that the present situa- tion leaves everything to be desired in regard to exact knowledge as a basis of procedure on the part of the State, if the Saratoga springs are to be effectively protected. With full realization of the seriousness of the problem there presented and of its difficulties, the State Geologist organized a resurvey of the Saratoga springs region during the past season. This survey was, of compulsion, corfined to a review of the sur- face structures of the country. It was fully understood that such an undertaking, unsupported by the drill, must be inadequate in its results, for in a subterranean problem the drill is the geologist’s finger. Appropriations, however, were wanting to carry on this extensive but essential part of the work. The records of the many commercial wells put down at Saratoga are lost or inaccessible, and no conclusions of the problem can be reached and no proper pro- cedure for the conservation of the springs be deduced until re- drilling over the extensive area has been carefully executed. The field work of the season was not, however, without good results in its bearing on the problems at issue and the survey of SIXTH REPORT OF THE DIRECTOR 1909 iW the Saratoga quadrangle carried on by Drs Cushing and Ruede- mann will be continued and concluded by being brought into con- nection with the survey of the Broadalbin quadrangle by W. J. Miller. . Referring specially to the field determinations made in this work, certain stratigraphic details have been perfected. The limestone of the Mohawk valley, which has heretofore been classed as “ Beekmantown,”’ proves to be composed of two unconformable members, the upper, comprising the so called “ fu- coidal beds,” a limestone of lower Beekmantown age, and the name Tribes Hill lunestone has been proposed for it; the lower is of dolo- mite, is older than the Beekmantown, and the name Little Falls _ dolomite is restricted to this member. The upper formation thins westward and disappears just west of Little Falls. In the eastern part of the Mohawk valley the Potsdam sand- stone appears beneath the Little Falls dolomite, grading up into it through a series of passage beds, the two plainly belonging to the same formation. At Saratoga the basal portion of the Little Falls dolomite becomes locally a fossiliferous limestone, which has _ been provisionally termed the Hloyt limestone. Over it the Little Falls dolomite, but the true Beekmantown seems to be absent, the - Trenton limestone resting on the Little Falls dolomite. Traced through Whitehall to Ticonderoga the latter is found to be directly equivalent to Division A of the Beekmantown division which lies unconformably beneath the remainder of the Beekmantown and does not belong with it but with the Potsdam and passage beds between. On the Broadalbin quadrangle in Fulton and Saratoga coun- ties, the area comprises rocks of Precambric, Paleozoic and Pleistocene ages. | The Precambric rocks cover about one third of the quad- rangle and are chiefly represented by the Grenville schists with which are associated vounger foliated syenite and porphyritic granite as well as nonfoliated dikes of gabbro or diabase. The remainder of the area is occupied by Paleozoic formations in- cluding the Potsdam, Little Falls, Trenton, Utica and Lorraine formations. Of the Precambric rocks the Grenville, in several distinct areas, is by far the most common, one area alone occupying more than 40 square miles. Belts of very pure quartzite are at times found in the Grenville. The syenite and granite are highly 12 NEW YORK STATE MUSEUM metamorphosed, the syenite commonly appearing almost schist- ose. The true Beekmantown appears to be absent from the Broad- albin quadrangle so that the Trenton always rests unconform- ably upon the Little Falls dolomite. A series of distinctly trans- itional beds lies between the Potsdam sandstone and the Little Falls dolomite. This formation has been named from the town of Galway where it is best shown and it has been separately shown on the geologic map. Toward the southeast the Pots- dam has at its base a very interesting conglomerate made up of Grenville quartzite fragments from 1 to 3 feet in diameter. The district is remarkable for its faults, no less than 14 having been mapped. They are all normal with displacements ranging from 100 to 150 feet. Several of these have been map- ped for the first time, and one of these, the Batchellerville fault, showing a displacement of 1500 feet, has been traced for over to miles. The Batchellerville fault is also of interest because, so far as known, it is the greatest of the Mohawk valley faults with the upthrow side on the east. Pleistocene deposits of various types are finely exhibited. There is distinct evidence, as shown by A. P. Brigham, that a cur- rent of ice flowing south-southwestward past Northville met another current flowing northwestward past Galway in the vi- cinity of Broadalbin. The lowest land, including the area of the great swamp known as the “ Vly,” was once covered by a gla- cial lake. | Adirondacks. Jast year I reported the completion of the survey of the Elizabethtown and Port Henry quadrangles by Professor Kemp and Dr Ruedemann and this report is now in press. Professor Kemp has followed this by the survey of the -Mt Marcy quadrangle which lies next west. The field work had been done upon the area in former years and the final re- port had been to some degree blocked out. This section of the Adirondacks contains many points of special interest. The two summits, Mt Marcy and Mt McIntyre, which alone of all the peaks exceed 5000 feet, are within it. Of the 16 peaks which stand between 4000 and 5000 feet, 14 are also here. The remaining two are Giant, which lies just east, and Whiteface which is a few miles north. It will thus be readily seen that we are here dealing with the culmination of the Adirondacks. : Careful study of the mountains brings out the fact that in the SIXTH REPORT OF THE DIRECTOR 1909 12 large way the ridges trend northeast and southwest, yet this general structural feature is modified by two broad north and south valleys, of which the larger, the famous “ Keene valley,” Gomtains the chief settlements and the smaller is marked by Elk lake. These latter valleys are believed to be old topographic depressions which have antedated the northeast and southwest faults, the causes of the later ridges. The northwestern portion of the quadrangle is occupied by a great gravel flat standing at approximately the 2000 foot con- tour and much cut up by the streams. Over at least Io square miles of area, no bed rock exposure is visible and one is forced to conclude that some relatively wide and open valley has been buried by the gravels which were incidental to the waning glacial period. The postglacial deposits and the moraines of the ice period it- seli have done much to modify the relief and rearrange the Siamese. There is good evidence of a lake that must have been impounded by some barrier on the north and that filled the Keene valley during the closing of the glacial period. The gravelly deltas along the sides of the valley admit of no other interpretation and in the case of the terrace on which the Willey House stands just beyond the northeast corner of the quadran- ele, the amount of gravel is so great as to be very impressive. There is little doubt that in the preglacial times the area around the Upper Ausable lake drained off to the southwest through the Boreas river and that drift has changed the old order of things. ‘The present divide is in a swampy area and is scarcely 20 feet high. There are many precipitous mountain fronts which usually trend northeast and southwest and afford beautiful scenery. In the narrow passes at their feet lakes may be situated, such as the Cascade lakes, the Lower Ausable, and Avalanche. Some of the mountains are also sharp and narrow in their summits, as in the case of the Gothics. Others, like Marcy, are rounded and dome-shaped. | The hard rock geology is similar to other Adirondack quad- rangles, already described in the bulletins of the State Museum. The oldest rocks are the Grenville sediments which are well Shown in the Keene valley. Except for one small patch, ap- parently caught up in the anorthosites just south of the Cas- cade lakes, they do not appear outside this depression. They may, however, lie buried beneath the gravels of North Elba and also of the Elk Lake basin. ; 14 NEW YORK STATE MUSEUM The rocks next in age are the anorthosites, which cover al- most all the quadrangle. They are its characteristic rock and constitute all the high peaks but one. The blue labradorite rock, sometimes giving opalescent coiors in the brooks, is al- most universal. The syenite series enters from the north and in a variety that is transitional to the anorthosites constitutes Pitchoff mountain. The syenites soon fail, however, and the anorthosites take their place. The anorthosites are cut by a number of intrusive masses of basic gabbro, of which the wonderful dike at Avalanche lake is a striking example. It runs from the lake to the summit of the ridge, cleaving two mountains apart like a wedge. | There are numerous basaltic dikes which favor the north- easterly fault cracks. The intrusive anorthosites have wrought some contact ef- fects upon the old Grenville limestones which are among the best illustrations of these phenomena yet noted in the Adiron- dacks. The limestones have been changed in one locality to masses of red garnet and green pyroxene, and in another have a body of magnetite much mixed up with garnet and other contact minerals. The ore body was mined to some extent in the old days of the forges but is now idle. It is the only ore deposit worthy of mention yet found in the quadrangle. The ereat predominance of the anorthosites would lead us to antici- pate only titaniferous ores outside of the Grenville area. Mineral wealth is thus lacking. The entertainment of sum- mer visitors and the lumber business are the chief means of support of the inhabitants. Southeastern New York. In my report of last year refer- ence was made to cooperative undertakings with the New York City Board of Water Supply, with reference to the assembling of the geological data recorded in that great engineering enter- prise. During the year past, Dr Berkey has brought together from these sources and from independent surveys of the contigu- ous territory, begun before this form of cooperation was effected, the general summary of new knowledge in the form of a bulletin which has been submitted for publication. In the preparation of this bulletin the immediate object has been to place in con- venient form an outline of the present understanding of the geology of the region and to discuss facts gathered in this ex- tensive exploratory work carried on along the course of the Catskill aqueduct, with special reference to the geological structures on Man- SIXTH REPORT OF THE DIRECTOR IQOQ 15 hattan island. The task has proven a difficult one. It has been found necessary to summarize the data and give results rather than to present the whole mass of facts. The final outcome will be the solution of a series of problems very largely in the form they have presented themselves to the practical engineer and others working on them. The bulletin therefore falls readily into the line of applied geology and it is believed will have dis‘inctive educa- Memaleitse in that field. Detailed study of old drill borings in New York city has led to the opinion that the present conception of the areal and struc- tural geology of Manhattan island and the East river needs con- siderable correction. This, however, applies only to the southern portion under heavy drift cover. The tunnel developments of the city make details of this sort of much importance. Instead of the island being wholly Manhattan schist, the data seemed to require that at least two narrow belts of the Inwood limestone and Fordham gneiss should extend through the lower east side. Ex- plorations designed to test this theory have proven it to be true. Limestone does not follow the East river continuously. A large area of grano-diorite cuts through the gneisses in Long Island City and Brooklyn and crosses the East river into Man- hattan. A corrected map of this section will be published in the bulletin. The exceptional advantages offered by tunnels now being con- struc:ed throughout the Highlands region along the aqueduct makes it possible to see the prominence of some structural features that are otherwise obscure. Faults and crush zones and other effects of movement are surprisingly numerous. They are in all stages between complete recementation and complete decay. Some of the older are in as good physical condition as the original wall rock, others of later origin are reduced to clay or similar incoherent matter to great depth. In at least one such case on Manhattan island, complete decay extends to a depth of over 300 feet. Additional exploration on the Hudson river indicates clearly that there has been glacial widening of the preglacial gorge at the Storm King entrance to the Highlands and that there is probably also glacial overdeepening. Borings in the channel have penetrated silts, sands and drift to a depth of — 674 feet at which point it is now believed rock bottom has been en- countered, 10 NEW YORK STATE MUSEUM Further detailed field observations tend to confirm the opinion previously given that metamorphosed sediments constitute the most ancient rock types of this region and that they are the equivalents of the Grenville series as known in the Adirondacks. Work on the Poughkeepsie quadrangle has been carried forward by Prof. C. H. Gordon, who reports as follows: Precambric. Some portions of the gneissic areas were fre- viewed with care. It has seemed entirely possible to establish the identity of the rocks which make up the narrow strip that ex- tends from the carpet mills at Wolcottville northeastward to Vly mountain with the gneisses of the Fishkill mountains. This strip, which will be referred to as the Glenham belt, was de- scribed by Mather as the “ Matteawan granite.” The rocks which make up its major portion vary from greenish granitic types of rather massive character to more gneissoid and usually somewhat finer grained rocks with reddish color. The primary minerals composing these two varieties are quite simt- lar and are quartz, microcline or orthoclase, plagioclase and bio- tite. The last named has undergone alteration which appears to be an ancient character. During the period of this alteration the biotite was more or less completely changed to chlorite and considerable quantities of iron oxids were liberated. Occasion- ally the granitic rock passes into a type with scarcely any ferro- magnesian minerals, with milky quartz and a feldspar pink from disseminated iron particles. These varieties grade into one another although the greenish rock is most abundant in the southern end of the strip and the gneissoid type around Vly mountain. The varieties just described are those which have Belen emphasized by most pues" and have been called “altered sandstone,” “bastard granite,” etc. Within the last two or three years new cuts have been opened in this strip in the process of evening up the grade on the road from Fishkill village to Wappinger Falls. This road cuts the strip about midway of its length. Among the rock varieties exposed in these cuts are hornblende and micaceous gneisses quite similar to some of those seen in the Fishkill mountains and several varieties of altered gneissic derivatives. Epidote 1s abundant in many outcrops. It has proved possible to trace in a satisfactory manner the rocks composing this strip through somewhat similar masses lying at the south in Matteawan to the base of the Fishkill moun- tains. Rocks identical with the altered and epidotic gneisses SIXTH REPORT OF THE DIRECTOR I909 D7: and greenish and egneissoid rocks of this strip were found in the eastern part of the town of Matteawan. Certain easily marked faults have broken the areal continuity of the whole. The Glenham belt near Vly mountain shows a small patch of the quartzite. In Matteawan a considerable knoll of the basal quartzite is preserved between Anderson, Grove and Walcott Pemecroiear ikock hollow.” The Precambric age of these masses is thus indicated. The Glenham belt and the smaller masses at the south are interpreted as inliers of the older rocks. The Glenham belt is a faulted inlier. The others are probably such. The rocks which make up the larger part of these inliers are looked upon as altered derivatives of the gneisses. They belong to the same general epoch as the quartzite, that of the transgressing Cambric sea. Their present compact condition is due to the same metamorphic processes that changed the basal sandstone to a quartzite and the overlying limestones and slate to their present condition. At Hortontown, a small hamlet in the Highlands south of Shenandoah, a basic eruptive made up chiefly of hornblende and magnetite, with some pyroxene, is in close association with a quartzite, entirely similar to the basal quartzite and of consider- able extent, and with a few scattered ledges of an altered rock made up of magnetite and bastite. The relations are very ob- scure. The presence of a clear fault along the eastern base of Shenandoah mountain seems to permit the interpretation that the eruptive is of Postcambric age and that it has penetrated the basal Paleozoics and altered the ferruginous dolomite with-. out materially affecting the refractory quartzite. Most of the altered limestone has been removed. ‘Cambric. The discovery of the opercula of Hyolithellus micans Billings in the bluish gray limestones overlying the basal quartzite at the base of the Fishkill mountains during the previous years, indicated that fossils in the quartzite would prob- ably be found in the neighborhood, and a slab of compact quartzite with the surfaces covered with brachiopod and trilobite fragments has been found in the yard of Ward Ladue in the West Fishkill Hook dis‘rict south of Johnsville. This find led to a per- sistent search for the quartzite in place. A few weeks later the fos- sils were found about %4 mile to the south. The locality may be reached by taking the east road into the mountain from the West Hook, passing the house of Ward Ladue as far as Herman Adams’s 18 NEW YORK STATE MUSEUM house, and then by following the gully east of the road for two or three hundred yards. The ledge occurs on the east of the gully about 3 or 4 feet below the base of a stone wall that separates the gully from an old orchard on the east. The fossils occur in the hard com- pact quartzite similar to that in Ladue’s yard, bu: are most numerous in the thinner, somewhat friable rusty layers just beneath. ‘The compact rock shows dull imperfect surface markings and numerous rusty spots when broken. The friable layers show ereat numbers of fragments including brachiopods resembling Obolella and the spines and cheeks of trilobites identified as Vem edikiurs: apace eR The basal quartzite passes conformably into a bluish gray. fossiliferous limestone in the orchard of Ward Ladue and north of here on the farm of William L. Ladue the limestone grades upward into calcareous shale thus giving a conformable series of Lower Cambric strata. Just what the relation of the lime- stone further north is to this series, it is very difficult to deter- mine. The Lower Cambric is probably faulted up into younger limestones. if Wappinger limestone. This formation occurs within the quad- rangle in two well defined masses: the composite Wappinger creek belt and the Fishkill limestone. A portion of the former was reexamined during the past summer for the purpose of learning more about the cherty dolomitic limestone overlying the arenaceous beds carrying Lingulepsis cf. pinniformis in the western strip of this composite belt. Apparently the latter beds grade up into the dolomitic rock. The latter does not appear to bear much resemblance to the so called “ Calciferous” of the central strip of this belt as déveloped at the type locality at Rochdale. Pass- ing westward along the Spackenkill road from the Albany post- road one crosses the gently inclined or horizontal Upper Cam- bric beds at points near Ruppert’s farmhouse and just a little east of this place, and then over very different cherty strata without fossils in which the stratification and dip are not dis- tinct. The two, however, appear to be in conformity. Near Camelot station the arenaceous Potsdam beds appear pitching to the southward and south of here at the Clinton Point Stone Company’s quarry at Stoneco are strata very similar to the cherty beds just described, with westward dip and such general position as to indicate that if continued northward they would have a position with reference to the Upper Cambric like that SIXTH REPORT OF THE DIRECTOR IQOQ Ig occupied by the cherty beds along the Spackenkill road. The thick masses in the Stoneco quarry have not yielded fossils. It seems that within this western strip there is a considerable thickness of heavy dolomitic limestones lying above the Upper Cambric fossiliferous beds which are older than the Beekman- fowiree. Calciferous,” Rochdale group). Whether this mass belongs with the Cambric of the Canadian group could not be deter- — mined, nor the question of whether deposition was continuous from one period to the other. During the seasons of 1908 and 1909 a number of new cuts were opened in the Fishkill limestone in the process of con- structing the State road from Fishkill Landing to Beekman. _ These were examined with considerable care, but except for one or two doubtful cases, no fossils were discovered. A mile west of East Fishkill (“ Gayhead”’) a slightly distorted impression with form suggesting some member of the Strophomenidae was found on the freshly broken rock. All shell characters were absent, although the form was reasonably distinct. Fossils which could be recognized have been discovered in this limestone along its western margin, in the Lower Cambric horizon, as above described, and in one instance along its north- ern margin near Hopewell. Elsewhere they have not been found either on fresh surfaces or in weathered outcrops. The slate formation is almost completely eroded from this limestone mass. There is reason for thinking that much of the limestone is older than the Trenton and perhaps of Cambric or early Ordovicic age. Hudson River siate formation. A careful examination of many outcrops in this formation has added only one new fossil locality. This occurs at a hamlet known as Swartoutville, about 214 miles north of Brinckerhoff. The fossiliferous ledges were discovered while tracing the limestone boundary. On the farm of Irving Hitch- cock at Swartoutville, about three or four hundred yards west of the road from Brinckerhoff to Hopewell Junction, is a high knoll made up of gray limy shales with interbedded limestones. The shales contain Plectambonites sericeus and other fos- sil fragments. These beds are regarded as lying near the base of the slate formation and as of probable Trenton age. The beds ap- pear structurally to belong with the limestone which is faulted against the presumably younger slates on the west. Considerable interest attaches to the discovery of several small, usually conglomeratic, limestone patches within this formation. Three of these occur near Arthursburg north of 740) NEW YORK STATE MUSEUM Tlopewell Junction and three somewhat larger ones east of Pleasant Valley. All appear to be brought up by faults within the slates. Several are marked by a limestone conglomerate entirely similar to the Trenton conglomerate of the Wappinger creek belt and Solenopora Compa eta. wacmoted tmece most western masses. ‘These patches are now exposed because of greater thrust at the points where they now he along extensive thrust lines. The conglomerate is often overlain by a silicious lime-sand rock which is followed by the slate formation. As far as it: goes the evidence would appear to show that at the east the lime-mud rock with fossils shown at Pleasant Valley, Rochdale and at Sleight’s farm near Manchester Bridge gives way to this coarser silicious sand rock. Close folding and prob- able thrusting have brought these two phases of contemporaneous deposition into closer areal relations than they had originally. It seems likely that the epoch of limestone formation during the Trenton transgression within this quadrangle was of short duration. Much of the slate is probably of Trenton age. Surficial geology Some reference has already been made to these features in Saratoga county and additional work was done on the general field of the lower Mohawk valley region over the Broadalbin, Gloversville, Amsterdam and Fonda quadrangles by Professor Brigham. This continued field work has brought to an essential completion the classification and distribution of the surface deposits in this region and the necessary maps and report have been rendered. Extension of this survey was carried into the area north of Gloversville, a district belonging to the southern Adirondack forest and lying in the towns of Mayfield, Bleecker and Garoga in Fulton county, and including the southern parts of Benson and Arietta in Herkimer county. The region is rugged, in large part wooded and attains a maxi- mum altitude in Pinnacle mountain, of 2514 feet. Many other elevations approximate this altitude. The valleys and slopes are covered with a massive and fairly constant mantle of glacial drift. Rock outcrops’ are fneqtent) but the averase thickness of the drift is-large. Distinctly morainic accumulations are, however, not important though some low hills of this nature occur about Bleecker, Bleecker Center and Lindsley Corners. Lakes and ponds are numerous, and belong in the main to the glacial blockade type, though it would often be hazardous to affirm that glacial erosion did not enter as a component factor. SIXTH REPORT OF THE DIRECTOR IQOQ 21 The chief interest from the point of view of the glacial geology is in the direction of the striae, records of this nature being found in about 24 localities. It is known that the movement a few miles to the south, about Gloversville and Johnstown, was westward, while the latest movement on the east, or about: Northville, was southward. The average movement in the dis- trict now studied proved to be southwest, showing that the higher grounds, well into the southern Adirondacks, felt the influence of the great westward movement up the Mohawk valley. The direct southward flow at Northville seems to have been late and in the control of the local trend of the Sacandaga valley. The top of the Pinnacle, on account of weathering, does not show distinct gravings, but the molding shows clearly a southwest trend. One mile north of Rockwood, on the edge of the Lassellsville quadrangle, the striae even show a direction of Ww. 20°-25° n. So at Wheelerville, near Canada lake, and by Middle Stink lake, also on the Lassellsville area, readings are approximately west. Aqueo-glacial drift was very nearly absent, the chief exception being in some interesting glacial terraces about Bleecker Center. The further extension of these Mohawk glacial waters was studied in a broad way by Professor Fairchild from Taberg in the Ontario basin to Coxsackie in the Hudson valley. The work was partly in review of critical localities and partly new mapping of the glacio-lacustrine features. It was found that a series of glacial stream channels lie along the west side of the Hudson valley, in continuation of the stream flow across the northeast face of the Helderberg scarp. Special problems Clinton formation. The value of this term in the geological nomenclature of America has been a matter of some general interest and discussion and as the term is an historic one, based on a rock section at and near the village of Clinton, the signifi- cance of the name and its proper definition may be briefly referred to. It would be a matter of slender and local importance if this rock series and the fauna it contains were confined to the State of New York, but as the division was early established by the New York geologists and the formation extends very widely beyond the boundaries of the State, northeast, southwest along the Appalachians, and broadly through the west and northwest, its definition assumes an importance of some magnitude. 22 NEW YORK STATE MUSEUM The Clinton formation was first called, by Vanuxem, the Pretean group, on account of the variable character of its sedi- ments and their colors. When, soon after, the geographic term Clinton was substituted for the formation, it was based on the rock section referred to at Clinton village, its lower limit being recognized as bounded by the Medina sandstone there present, but its upper limit being undefined, or in other words, the entire section there exposed above the Medina formation being left as the exponent of the Clinton formation. In the Genesee valley the Clinton term was also recognized and used contempora- neously by Hall. There the formation is much more advantage- ously and completely expressed, and over it lies without inter- ruption a bed of gray shale which was separately Beas by Hall as the Rochester shale. Our knowledge of the fauna of the Clinton unit, as well as of the Rochester shale, has been essentially derived from the Genesee section. With the progress of knowledge it is satis- factorily determined that at the Clinton section at ‘Clinton is a weak development of the Rochester shale and this was included by inference in Vanuxem’s definition of the Clinton formation. In actual date of establishment the term Rochester shale is older than Clinton, but only the work of later years has shown the presence of the earlier named- formation im thes toe section of the latter. The question has, from these acknowledged conditions, arisen in this form: Shall the Clinton formation be made to include the deposits and fauna of the Rochester shale? In New York we have felt disposed to hold the view that the early geologists, of course totally unaware of the sharp and pre- cise requirements of an advanced knowledge, employed forma- tional terms with some degree of elasticity, even of laxity, and in the particular case in hand, that the rock succession ime Genesee valley is a truer demonstration of actual relationships and its early denominations a more faithful expression of suc- cessive geological events than either section or names in the Clinton section. It seems to us doubtful whether ancient and loosely defined names can wisely be resuscitated, in defiance of advances in knowledge, or whether such attempts at resuscita- tion are not virtually new definitions, thus lacking wholly the merit claimed for their age. The stratigraphic contrast in these two sections is very pro- nounced. In the Rochester or Genesee river section the Clinton Seth REPORT OF LHE DIRECTOR I1Q0Q * 23 beds from below are as follows: (1) Sodus shale, (2) Furnace- ville ore, (3,) Wolcott limestone, (4) Williamson shale, (5) Ironde- ‘quoit limestone. In the Clinton section no entirely satisfactory division of the strata has yet been made. How far the divisions of the Rochester secticn can be correlated with or applied to the Clinton section is still to be determined, but they now seem to have little in common. The Wolcott limestone is certainly not repeated in the section at Clinton, and the presence and extent of the other divisions can be determined only by careful study of the intervening area. At Clinton there is an important stratigraphic and faunal break at the top of the green shale overlying the lower or oolitic ore bed. the shale is here overlain by heavy liraestones showing traces of Deewamd O teet higher is the upper ore or red flux bed. The fauna of this section indicates the presence of species of the Rochester member well down in the strata and in paleontology it may be unwise to separate the Rochester member and its fauna from the series with which it is so intimately bound in this typical sec- tion. To expand the group value of the term Clinton by the ad- dition of the member Rochester involves a subtraction from the Niagaran group in like degree. This procedure may be necessary however as it is evident that final resolution of the original Clinton will leave no element that can serve as a Clinton member, except perhaps the ore beds which have long held wide recognition in the Appalachian region as the Clinton tron ores. Dikes near Clintonville, Onondaga co. Dr Burnett Smith of the geological department of Syracuse University has recorded in Science (Nov. 19, 1909) his recent discovery of heretofore unknown igneous dikes in the sedimentary rocks of Onondaga county. Dr Smith’s notice follows: The presence of a few igneous intrusions in the almost undis- turbed Paleozoic strata of central New York has long been known to geologists. Their extreme rarity, however, has always invested them with a peculiar interest. Excluding the Manheim dike, near Little Falls, which lies about 75 miles east of Syracuse and which cuts Ordovician strata, we find that these igneous rocks may be grouped geographically into (1) those occurring in the vicinity of Ithaca and Ludlowville and (2) those occurring in the vicinity of Syracuse. In both regions the intrusions are peridotite and are mostly true dikes cutting in the first case such Upper Devonian formations as the Genesee shale and the Portage and Ithaca shales and sandstones, and in the second case cutting the Salina beds of Silurian age. 24 NEW- YORK STATE MUSEUM As far as the writer has been able to learn, the geologically intermediate Hamilton shale has, until now, yielded no dikes and the recent discovery of two in this formation at a locality about 12 miles southwest of Syracuse and about 40 miles northeasterly from Ithaca is believed to be a matter of interest. The dikes in question are exposed on the south wall of the Clintonville ravine at a point approximately 50 feet above the level of the Marietta road. The more western is a fine grained porphyritic rock resembling peridotite. What appear to be ser- pentine grains, produced by the alteration of olivin, protrude from the weathered surface and have the appearance of small pebbles. Another conspicuous feature 1s furnished by large scales of a bronzy mica. This dike has a uniform width of from 7 to 8 inches and is displayed for about 12 feet on the south bank of the ravine. On the north side it is obscured by talus: Its plane is vertical, while its direction is north and south, agreeing in this latter respect with the Ithaca dikes. Wherever examined it presents a very uniform texture, is apparently free irom iras- ments of the sedimentary rocks through which it passed, and has produced little contact metamorphism. The second dike discovered by the writer lies about 2 feet and 4 inches to the east of the first and was not observed until the wall at this point had been cleaned. It has a width of about 8 inches. Like the first dike, it is vertical and north and south in direction. It differs, however, from the first dike in being much weathered in places and in containing many shale fragments some of which have a long diameter of 3 inches or more. Dr Smith has, at my request, supplied specimens from these interesting occurrences for examination by Prof. C. H. Smyth jr, whose acquaintance with the other dikes on the sedimentaries of central New York is intimate, and the latter has supplied some notes thereupon, essentially as follows: They are greatly altered alnoites. The olivin is completely broken down into serpentine, magnetite and, often, carbonates. At the same time, the mica remains surprisingly fresh, as it does in other dikes of the region. Perofskite, so abundant in the Manheim dike, is much less conspicuous here, while the critical mineral, so far as classification is concerned, melilite, is almost obliterated. One section from each dike, however, shows what I consider quite unmistakable traces of melilite, in one case a good deal of it, and I have no doubt that if the material were entirely fresh, the rock would prove to be quite typical alnoite. At first glance, it may appear that the presence or absence of melilite is a trifling ma‘ter, since, at most, it probably would be only a minor constituent, the rock consisting chiefly of olivin and mica, and thus, for the most part, resembling, if not belong- ing to, the peridotites. But, really, the question is of more than ordinary interest, for as soon as melilite appears in an olivin rock SIXTH REPORT OF THE DIRECTOR IQOQ 25 of this type, we are dealing with a rare variety, which is rarely found except in association with nepheline-syenite. From this it follows that the presence or absence of melilite, instead of being a mere matter of one mineral more or less in the rock, determines the la:ter as belonging in the alkaline or subalkaline group, as the case may be, the peridotites belonging in the latter class, the alnoites in the former. Now as this dis- tinction, recognized by Iddings nearly 20 years ago, and recently emphasized by Harker, is probably the most fundamental and far- reaching subdivision of igneous rocks that we have, it is, of course, a vital matter in the history of these dikes to determine in which group they belong, and the whole matter turns upon the one mineral —melilite. If the rocks contain melilite, they are alnoites and in Memdicalime, Of, to use Harkers term, Atlantic group. On the other hand, if they contain no melilite, they are peridotites and belong to the subalkaline or Pacific group. As these groups are not only of the first order of magnitude, but, as shown by Harker, may be genetically connected with major types of crustal move- ment, there is a heavy responsibility resting upon this one re- grettably unstable mineral. Rock cities of Cattaraugus county. It is not generally known that these singularly picturesque exhibits of rock decay are en- tirely unique among the scenic features of this State. New York is well supplied with striking scenic effects resulting from the more usual procedures of natural forces; cataracts and erosion gorges, ravines and chasms, mountains of grandeur and stock- aded cliffs; natural rock bridges and subterranean caverns. These rock cities, however, particularly that situated a few miles south of Olean, Cattaraugus co., are phenomena of an- other order, wherein the decomposition of the rock beds under meteoric agencies has broken and gashed the rock beds into extraordinary picturesque effects. Their unusual features at- tracted the special attention of the geologists at the time of the original survey, 1836-42, and Professor Hall made an extended reference to them, accompanied by a series of effective sketches drawn by Prof. Eben N. Hosford, then his field assistant. These rock cities are situated high on the summits of the hills and in the days of the pioneer survey were accessible only with difficulty. The growth of population and facilities of inter- course have now brought the most striking of these, that near iiesim, ito easy reach of the public, by ‘means of a trolley system running thence to Bradford, Pa. over a route of rare pictur- esqueness. The Olean rock city is happily under control and protection from the encroachments of timber cutting and oil drill- ing which had begun to attack it. NEW YORK STATE MUSEUM 26 YWno, ey} Jo Wodey jessopost) 24} Ur P ‘Ajuno0d AUeSIT[V Ul ‘UvaTCO JO YNos sar g- EVR ‘yO1t4sSIC aystjqnd ‘projsiop{ “N “A “ford Aq yoyoys B Woy ‘QYeIIWIO[SUOD IY} JO 9Spo UTOYJIOU OY} FO YAS ———— == a SS SSS SaaS S535 Stars ae} = N = 2 = es = = IS ee <= : ISS A SN cola =a S : : Z He ~~) —— SONADIO JUIOL YIM o}vJoWO[sU0D oy} Jo doy “APD YOY uvsO ed ies a oe | we i aa tis, ba He prea Br Pe oh es i > ‘ I 9}e[q d}eIOWO[SUOs s[qqod zjienb oyyM OY} JO ddVFING “A}IO YoY uvrszyo Z 938d uraO «YY OL, “AWD yoy € 93eIq Olean Rock city. The bottom of a joint crevice due to decay Plate 5 Olean Rock city. Weathered crevice in the conglomerate Plate 6 ined by decay d conglomerate partly underm jointe The Olean Rock city. SIXTH REPORT OF THE DIRECTOR IQOQ 27, These rock cities consist of immense quadratic blocks of con- glomerate (Olean conglomerate of the geological series) which form the capstone of the broken plateau whereon they rest. The Olean rock city lies at 2400 feet above tide and is highest of them all. The procedure of erosion in cutting out the bound- ing valleys of these hills has left only remnants of this sheet of white quartz conglomerate, now broken up into giant parallel- opipeda by the slow action of atmospheric agencies working along original lines of structure. These structural lines are the vertical series of joint faces produced by shrinkage in and lateral strains upon the rock beds. The Olean conglomerate Which composes the Olean rock city, is represented here in very nearly its entire thickness in this State and although for a large part a conglomerate of rounded milk-white quartz pebbles, yet the intervening bands of deposits are fine quartz sand. There is nothing above this conglomerate except a few feet of sandy shale which are now embraced within the same geo- logical unit. This Olean conglomerate not only forms the cap- stone of these southern hills, but also the capstone of the New York series of geological formations, it being the highest and latest term in the Carbonic rocks of the State, corresponding in part to the Pottsville division of the Pennsylvania coal measure Beties, The easy decomposition of this rock is due to the fact of its singular weakness of cementation. The pebbles and sand grains are held together, not by any calcareous binder, but by a faint and tenuous deposit of silica derived from the solution and redeposition of the quartz pebbles themselves. So feebly are both conglomerate and sandstones bound that an easy blow, often no more than a hand pressure, will separate a frag- ment. It would appear therefore that time has still been want- ing for a firm cementation by redeposition of a secondary silica, NEW YORK STATE MUSEUM 28 Crgi “LISI YIINoY oy} JO JAoday Jeorsojoex) sy} ur poysrjqnd ‘DIOFSIOW “N “A JOIg Aq yOpoYs @ WOIT “ayfLAIoonpy JO YMos soprur 4 “Az YOY UL Met — ——- = = == =—— = SSS a —— > Sa a fp pred Ta ~ = fae D === SS SSS Wt y P i “ii = = — = OS, y iff ——— “ i eS 1 i Lilli z ", Alt FL a — _——S=S= —- —— LSS = = = ————— —SSaeSSSSFSS—_S9 ——— SS — iN ast Se Bs a unl = a cl mi nN Hh Poses ANT SS —= —- Olean Rock city. A weathered joint crevice Plate 8 Olean Rock city. “The Swine’s Snout” BUIIOUJVOM [CJUOZIIOY pure [VIT}IOA “APO YOY uvoio SSEU [VN PIsol PoyejOsl Ue ‘Yooy suo ,, RE EAT ee SE cet : i ee oe D, “AYID YOY Uvos[O eo ep Ol 93¥[qd Cecilia ian Plate 11 “one Rock ~ Olean Rock city. SIXTH REPORT OF THE DIRECTOR IQOQ 29 or that, the secondary silica has of itself been less resistant to atmospheric decomposition than the primary vein quartz of which the pebbles are apparently constituted. Yet it is not necessary to regard this secondary deposition as a large factor in cementation. Indeed cementation here has chiefly been effected by secondary crystal growth of the constituent pebbles. Some investigators have thought that the conglomerate pebbles displayed general evidence of etching under the action of organic acids. ‘The eye is attracted at once by the glistening surface of these pebbles, reflecting the light from a multitude of facets, and these facets are all of crystal growth. Indeed pebbles are easily found wherein this crystal enlargement has gone forward to almost complete construction of the simple prism and pyramid with the original rounded pebble visible as a nucleus. This enlargement is general throughout the deposit and implies room between the pebbles for such growth; hence a very loosely cemented mass chiefly now held together by the locking of the secondary deposit. This general condition of weakness has been the cause of breaking down the rock beds wherever there are lines of slight resistance; thus principally along the almost rect- angular series of vertical joints the dissolution here resulting in quadrate blocks standing like masses of floe ice floating on the sea. Again easy passage through or between the strata has weak- ened and undermined the support of the blocks so that they have been tilted over at various angles. Thus the picturesque ¢hasms, the sunken grassy walks, the rock bridges and the danger- ous clefts are to be accounted for. Examination of the original quartz pebbles under the crust of Secondary growth shows sufficient evidence of the dynamic Strains to which they were subjected in the formation of the rock masses from which they were derived, but of the geo- graphical origin of these pebbles, what land it was that furnished them and by what lines of transportation they were brought hither are problems still remaining to be solved. Supposed gold sands of the Adirondacks. The past year has witnessed a recrudescence of interest in the alleged gold-bearing sands of the Adirondacks. This office is frequently called upon for information on this subject, as weil as for an expression of opinion regarding certain enterprises which have been inaugurated for the purpose of working such deposits on a commercial basis. - The occasion seems opportune, therefore, to publish a general Statement for the consideration of those who may have little 30 NEW YORK STATE MUSEUM familiarity with the geology and mineral resources of that region. It is not within our province to offer personal advice to prospective investors, but it is proper to set forth the results of investigation and other matters of record that bear upon the matter. There have been many attempts to promulgate a gold-mining in- dustry in the region. The thoroughness with which the prospector for precious metals has covered the ground is to be seen in the abandoned pits and diggings that are scattered over every section. During the Klondike excitement, 10 or 12 years ago, the Adiron- dacks became the scene of a veritable rush for gold and practically every available sand heap was taken up for exploration. In the year 1898 alone there were filed nearly 4000 claims to gold and silver discoveries in the State, mainly within the Adirondacks. The basis of all this activity is the alluvial and glacial sands which occur in almost every stream valley. These sands are not derived from remote regions to the north—though the opinion seems common that they have been transported by ice from Canada and even from as far away as Alaska— but are the result of erosive agents working upon the local rocks. They consist entirely of the minerals of the country formations which are chiefly gran- ites, syenites, gabbros and gneissoid rocks of very ancient origin. Along with the lighter components, quartz and feldspar, there is a small proportion of the heavy minerals like garnet, pyroxene, hornblende and magnetite which have sometimes been separated by water action into distinct layers and which are found as black sands along the shores of the Adirondack lakes. It is in these heavier concentrated portions of the sands that gold should be found if present anywhere in the region. Assays by reputable firms have occasionally shown a small quantity of gold, ranging from a mere trace to perhaps $1 a ton. The examination of innumerable samples under the microscope has failed to reveal any of the precious metals, though of course such evidence is not conclusive as to their absolute presence or absence. On the other hand the claim has often been put forth that the common quartz sands in certain places carry from $2 to $20 a ton, which, if true, would under ordinary circumstances bring them into the zone of practical exploitation. The statement is commonly made by interested parties that the fire assay is unsuited to the determination of gold in these sands and special analytical methods ‘must be employed. To this it can only be said that the fire assay has stood the test of long practice SIXTH REPORT OF THE DIRECTOR IQOQ oil in all the mining regions of the world. No reasonable explanation for its failure in the present instance has been forthcoming, though by the use of such vague terms as “ volatile gold,” “ atomic con- dition and “chemically combined gold,’ there seems to be an implication that the gold is driven off or left untouched by the fire. As a rule the gold found by fire assay is several per cent more than the amount extractable by the most refined commercial processes. The exact methods for the recovery of the gold have usually Deemekept Secret, out of the reach of scientific inquiry. They, rather than the mines themselves, seem to be the principal con- sideration in the organization of these ventures. From such in- formation as has been given to the public, it would appear that they are generally based on some variation of well known methods or are a combination of processes in use elsewhere for gold recovery. A good example of Adirondack practice, if it may be called such, is to be found in the so called Sutphen process which was in vogue about Io years ago. Mulls of ambitious design were erected at Hadley and Glens Falls for its exploitation. It involved pulverization of the sand, treatment with a secret solution, and amalgamation. The necessity for grinding the sand, already in a fine state, was alleged to be the distribution of the gold in the interior of the quartz grains. The success of the treatment, how- ever, hinged on the character of the chemical solution, since the metal was stated to exist in combination with bromine and had to be set free before it would amalgamate. So much information was vouchsafed by the principals of the enterprise in an investiga- tion by this Survey. A sample of sand taken from the bank from which the mill at Hadley was supplied showed by fire assay only a trace of gold, or less than 25 cents a ton, and no bromine. The enterprise received a great deal of attention during its brief career. The yield from the mill was said to have been as high as $7 a ton, and the working costs only $2.50—a handsome margin of profit for gold mines of the present day. It would appear as a matter of general experience that a neces- sary condition for the supposed widespread distribution of aurifer- ous sands is the existence of quartz veins or other deposits of primary nature to which the sources of the gold could be traced. So far these have not been found, and in view of present knowledge of the Adirondacks, it seems very unlikely that they ever will be discovered. The quartz veins that occur in the region partake little 32 NEW YORK STATE MUSEUM of the characters of those found in gold-bearing sections, being essentially destitute of iron sulfids and other minerals with which the precious metals are most generally associated. That they con- tain traces of gold is likely, but they do not afford any adequate basis for mining enterprise (except as possible sources of quartz) or for the accumulation of secondary deposits like placer sands and gravels. There is little need for going further into details in this matter, though it may be said briefly that the Adirondacks form an inde- pendent geological and mineral province, only remotely related to the other mountain ranges of the eastern United States. The fact of the existence of gold deposits along the Appalachians from Nova Scotia to Alabama can scarcely be quoted, therefore, as an argument for the presence of analogous deposits in the Adirondack region. While deficient in the precious metals, the region possesses the elements of large mineral wealth. Its production of iron ores, talc, garnet, graphite, pyrite and building and monumental stones of various character is a very important contribution to the mineral output of the country. There is abundant opportunity for future development of such resources and it is in that direction rather than in the seeking of the precious metals that energy and capital can be best employed. The fact that the profits of mining are not to be gaged by the relative value of the mineral produced is a commonplace. If a balance could be struck, 1t would show probably that the homely iron ores better reward industry than all the gold and silver wherever found. Industrial geology Gypsum resources. With the growth of interest in gypsum and its products that has taken place in recent years, there has developed a need for a more thorough consideration of the New York deposits, commensurate with their commercial importance. Previous studies have afforded scarcely more than an outline of their field distribution and insufficient information of their char- acter and utility, as in fact for a lone time they were considered of small value except for local agricultural requirements. The discovery that the gypsum can be employed in the manufacture of calcined plasters has led, in the last decade, to the establish- ment of numerous enterprises, and there is every promise of a continued expansion in the industry for years to come. Recent field investigations have extended from Madison county SIXTH REPORT OF THE DIRECTOR 1909 33 west to Erie. The gypsum deposits are found in the upper part of the Salina formation which outcrops as far east as Albany county, but they attain workable dimensions only in the central and western areas where the Salina beds are thickest. Within this section which measures over 150 miles east and west they show a wide range of character, as one might expect; while there -is also considerable variation in the size and sequence of the bodies. Chemical analysis of various selected rock samples indicates that a relation more or less consistent exists between the com- position and geographic distribution of the gypsum. In general it may be said that there is a progressive increase in the per- centages of gypsum substance and a corresponding improve- ment in physical qualities as the deposits are traced to the west. This relation may be the expression of original conditions sur- rounding their accumulation which will later be considered. In the eastern counties the gypsum is admixed with clay, lime and magnesian carbonates and silica, the proportion of these impuri- ties ranging up to 25 per cent or more of the whole mass. On the other hand the deposits in the western part of the belt show as little as 5 per cent of foreign ingredients and are much lighter in color. The valuable bodies occur interbedded in the Upper Salina mealies. Phey occupy usually large areas, as compared with their vertical dimensions, or in other words are stratiform. There are, of course, variations and irregularities to be found, but the stratiform type is the predominant and original one; the extreme departures from that type such as have been de- scribed and figured in the reports of James Hall and in Dana’s Manual are in most instances to be regarded as modifications brought about by the solvent effects of ground waters. Besides the larger beds small seams of crystallized. transparent gypsum, which appear to be secondary depositions, occur through the shales, so abundantly distributed in some places that the mixed shale and gypsum has been worked during times past to supply local needs for land plaster. The forthcoming report will include a consideration of the Origin of the gypsum, a subject that has economic bearings as well as geologic interest. Without entering into details of evi- dence here, it may be said that the gypsum is considered an accumulation from sea water evaporation contemporaneous in ot NEW YORK STATE MUSEUM general with the deposition of the accompanying shales and limestones. The rock salt which occurs lower down in the Salina is a product of similar conditions. Owing to the seem- ingly abnormal position of the main gypsum beds with respect to the salt and to the occurrence of irregular discontinuous masses near the surface, the view has sometimes been taken that the deposits represent former limestones which after their uplift were altered to gypsum by underground circulations carry- ing sulfuric acid. If this explanation were true the resources might prove to be limited, since their existence would be depend- ent upon purely local conditions. It is to be doubted, however, if such methods of origin can be applied to the valuable beds of rock gypsum. Up to the present time the deposits have been attacked only at the more advantageous places on or near the outcrop. In the eastern section where they are thickest open-cut operations are the rule, while in Monroe county and farther west, they are commonly worked underground either from an adit driven from the face of a hill or by means of a vertical shart.) “Minesemiaae been little systematic exploration, but the need of it will come with the progress of the industry, particularly in the western counties which are the centers of plaster manufacture. The report will contain maps and other matter to indicate the more promising fields for future development. Review of mines and quarries. The canvass of the mining and quarrying enterprises of the State, relative to the year 1908, showed that conditions were less prosperous than in the few years immediately preceding which were reviewed. in former reports. The total value of the mineral production, itemized under 34 materials, was $29,519,785. The corresponding figures for the year 1907 were $37,141,006, so that the decrease amounted to about 20 per cent. . The lessened activity was not, however, attributable to factors of local import, but to the wide-reaching depression that affected all lines of business. An improvement will doubtless be shown by the statistics for the current year, though the industry can hardly be expected to regain fully its former activity in so short a time. The iron mines perhaps suf- fered most from the financial stress owing to the fact that many of the properties were still in the developmental stage and without the resources of established enterprises. The collection of the mineral statistics for the year was accom- SIXTH REPORT OF THE DIRECTOR 1909 35 plished with the cooperation of the United States Geological Survey, under the agreement published in my last report, the two offices sharing the work and the use of the results, Iron ore explorations. “~The Lake Sanford region, Essex co., was visited for the purpose of recording the recent develop- ments that have taken place since the issue of the report on the Adirondack magnetites. Exploration with the diamond drill has demonstrated the presence of many millions of tons of ore, thus confirming the general opinion relative to the resources of the region, Experiments in the reduction of the ores are still under way and their favorable outcome will mean a very large incre- ment to the mining industry of the Adirondacks. Examinations have also been made of the Forest of Dean mine near Fort Montgomery and of the arsenical pyrites mined near Carmel, Putnam co. SEISMOLOGICAL STATION The seismographs in the basement of the State Museum have continued to render efficient service, with only occasional stop- pages of short duration for the purpose of slight repairs or readjustments. Since their installation in March 1906 they have registered 54 different disturbances. The number registered during the year ending September 30, 1909, was 19 as compared with 9 in the preceding year. The seismic frequency has thus been rather notable,. equalling in.fact the record for the year 1907-8 which was distinguished by a series of very heavy earth- quakes in Mexico, the West Indies and Central Asia, that in- volved many minor readjustments in their train. The sources of the shocks in the past year have been fairly well distributed over the different seismic zones. The Cordil- leran region, after the repeated rackings that followed the San Francisco earthquake and extended from Alaska to Chile, seems now to have settled down to a more normal condition. Slight tremors only have been reported from that region. The loci of pronounced activity have shifted to the east-west zone which extends from the Mediterranean coast to Central Asia where there have been several heavy earthquakes; of the num- ber the Messina earthquake of December 28, 1908, involved the most appalling catastrophe that has ever been inflicted upon a civilized country. The shock itself does not appear to have been commensurate with the enormity of the destruction, the tracing obtained at Albany as well as at other stations showing 30 NEW YORK STATE MUSEUM no remarkable features. Within the same zone belong the dis- turbances of India, Persia and western Europe of which records are included in the accompanying table. As usual the local station has freely communicated its obser- vations to those engaged in seismological investigation and to the press. Facsimile reproductions of the San Francisco records are included in the final report of the California Earthquake Commission recently published by the Carnegie Institute. It is hoped that a systematic exchange of records may be inaugurated between the several stations in the eastern United States and Canada; the comparison and coordination of data from a number of observational centers would be highly desirable. In reference to the accompanying records it may be stated that the Albany station is equipped with two Bosch-Omori horizontal pendulums. One of these is set in the meridian and the other at right angles. The weight of each pendulum, includ- ing arm, is 11.283 kilograms and the distance of center of gravity from rotating axis is 84.6 centimeters. Their period is main- tained at about 30 seconds; their multiplying ratio is 10. They have no artificial damping device. Albany is situated in latitude N. 42° 39’ 6”, longitude W. 73° 45’ 18”. The base of the instru- ments is 21 meters above sea level. RECORD OF EARTHQUAKES AT ALBANY STATION, OCTOBER I, 1908 TO OCTOBER I, I909 Standard time Beginning Beginning Max. DATE prelim- principal Maximum End ampli- inaries part tude 1908 Jol ool h. m. Jal) ool. emma mm. OCtobersrse eee 12) 18.949 M0 22,20 ea eae) oneal t nar tloy a.m. 2 November 6........ 2 SOs Ca VIM all omen ei tens cite eam io cs ect ame aa 30 SS ae ees November 30....... 4 504 p.m 4 57% p. m 4 58\p. m. SB 643} jo) inal, 2 IDYegoM ley Ay — Ass wall wi AC) JO, say | Ge deokoooue I2 oo noon 12) Lovaeen: 4 1909 EDEN AGIOS Me Actsic oll ui) Sissy 10), sam TOMA 7 pe ts Io 474 p.m. IO 56\p. m. 2 HebrianyeuOr ese ET SO Vey Thy sl) BAe eee Per | aie aien aameeeet eae TOY) 713) cae | Pare February 26.:......| 12) 00) moon | (x2No5 1p. aia ime soni aipeena a seamen erat 1% JAN che Dh Colin ety sbeebs 9 ie Z2NOG) spate B) aie) 40), 1801. 27 Tom pe ia BBO On ial, I+ MASP TE SOAs ays waenishar: 8329) {py dn se aaa jncciet a eieaoy Mesto Nc Aatcgcrtps Pi eeron Onda WP aad Sa, WET Ae Nae etels ats Sv Quaraa aay Ain! els s90), Sy) 1G, hy coal 33 2S) Ble haat, S MANET Ocha crevauk Sito T2 03). MP SAL: WAG eee ca ena te aieaet ra eee ee Weary ASIN OW Ody ay wane ho INES < he TOG se TO eis ee ce a cee a | ae DPA Ovals oithcy |v eens Ul a yiane das ctor eet A. S54a0p.m: 3 @)ir © 1D, am. SOR iOs 1001, Bo ZS Top ran, 2 MUL SOL ths coves cee Ortele ets fy coal Oy siay” Bh, han 5) > Aly soa: 7 OOVae Th 24 Mttlyarshn vier. otucastos om A Bik 0), son, STAT irate Vg 40), sao aie) {O), 200, 6 SUI dst) TOR. ateneerals 2 Ou aan Oe heey Mel. sais 25TS aim 2 44a. m. 20 NATO TASE Bite ol seated: POO), {Eee Oe oe ae ee ere fe (Oye ER, 5001, Tada. Tet. oe September 8...... T.2)OOW MOON i): Vevanter see ee een ee ene TONG) JO aCe MP A September 22...... O4545 a. mM. || sro) oz) asm TOMOS yaar ibay Gio) ley i902 a SIXTH REPORT OF THE DIRECTOR 1909 37 October 13. The vibrations continued for nearly an hour and their east-west component was the stronger. They appear to have been set up by a distant shock, perhaps originating in central Europe, which was in a state of unrest at about that time. November 6. Very small vibrations of which only an east- west component was recorded. Severe earthquakes were - felt in Italy, central Europe and southwestern Asia at correspond- ing times. They were probably preliminary to the Messina dis- turbance of December 28th. November 30. Well marked though small vibrations of about equal magnitude on both instruments. Origin unknown. December 27-28. A record of the disastrous earthquake at Messina, Italy. The vibrations at this station lasted about 40 minutes and reached a maximum amplitude of 2 millimeters at 12 midnight. Only very faint movements were shown by the east-west pendulum. Other stations in this country and in Europe reported the wave motion to have been of moderate dimensions. The earthquake was due probably to crustal dis- location along the depression occupied by the straits of Messina. January 22. Record of devastating earthquake in the province of Luristan, Persia, in which 60 villages were wholly or partially destroyed. The shock was of world-wide compass and was re- ported by almost all stations. No direct news of its effects in Persia was received till February 17. The vibrations at this Station were of about the same intensity as those set up by the Messina earthquake, though they traveled a much greater dis- tance. No vibrations were indicated on the pendulum recording the north-south component. February 16. The shock traveled apparently in an east-west direction. The movements lasted for 17 minutes with oscillations of small amplitude. They may be referred to the violent shock that was felt throughout Alaska on the same day and ee from Skagway Lynn canal at 7.30 a.m. February 26. Record more clearly indicated on the east-west instrument. The epicenter is estimated at 2500 miles distant. The shock was also recorded by the Ottawa station. | April to. Record obtained only on the north-south instru- ment. The shock was of moderate intensity, with a maximum amplitude of 1% millimeters. Its origin is unknown but appears to have been about 6000 miles distant, possibly in the eastern Mediterranean region. | 38 NEW YORK STATE MUSEUM April 24. Slight oscillations of unknown origin recorded by both pendulums. May 17. Vibrations of moderate intensity; recorded also at Washington and Toronto. The origin is uncertain but has been assigned to Chile where earthquakes were felt at this time. May 18. A series of vibrations of moderate intensity travel- ing in an east-west direction. Their origin is unknown. June 8. Record of a slight earthquake which occurred in Copiapo, Chile. July 7. The disturbance can be traced to the: shock reported from various parts of India. The vibrations began at 4.54 p.m., which, with due allowance for difference in longitude and time of transmission, would correspond to about 3 a.m. at Bombay or be- tween 3 and 4 o'clock a.m. in central India. The movements were of small amplitude and continued for about an hour. As India is on the opposite side of the globe, the movements were probably transmitted across the polar regions as well as in an east-west direction. Stations in Russia, Germany, Spain and aaa also reported the same earthquake. July 30. Reston) = aaa WHITLOCK The Last of the Iroquois Potters. M. R. HARRINGTON Index Memoirs y 2 No. 9g pt 2 Early Devonic of New York and Eastern North America. Contents: Introduction Dalhousie formation Description of species Arenaceous Devonic faunas of Somerset, Piscataquis and Penobscot counties, Maine Description of species Devonic faunas of the Chapman By John M. Clarke. _ Notes on the Oriskany fauna at 250p. 36pl. 4 maps. Highland Mills Table of the Oriskany fauna of New York-New Jersey region General conclusion Supplementary notes Fault and infall at L’Anse au Sauvage on the Forillon, Plantation, Aroostook county, Gaspé | Maine Crinoid from Grande Greve Description of species limestone Early Devonic in eastern New | Explanation of plates York Index - Bulletins Geology 3 No. 126 Geology of the Remsen Quadrangle. Bis £ Miller. 54p. I1pl. map. Contents: = The Precambric surface Introduction Absence of the Dolgeville General geologic features Topography and drainage Rocks of the region Structural features The Paleozoic overlap (Upper Trenton) shales Glacial geology Economic geology Index eo) ve} =) se) SCUId 40 ADO TOALSO vine LAN \\) ENOLS ONIGTINGs Ze NEY LOH. -fy SAVCINOINO — ree em a nes eee er ra , x = ped \\ ey SHLAW 2) ( HOAAAN dd SHLLITOLdVY = ISTO TOWOING “Ldte 62 = —— a SINONSL Ay > WS HIXON NUBLSVE 9S OX ANG 20 SINOASC ATEWE® | caeus UNWIMOOM CNY s AVE ONLLOSdAY SLOBGNI® SHAUL UNVTCOOM UNV =< Wuvd ONILOGdY SLOASNI® O S \\aTa HIWON H) SINV Id | SiSdd GauL GCVHSN \\ \S.LOSSNI 30 NOLIWAUTS Td S \\ [S68] LSINVLOG ‘Ldau WOON ailaad Ave) Wid © \ STISSOd do SNSWIOGES BdAL \ Suddvd TWold0 \ \ \ \|SNolLoat109 TWI1507029 > SHONOdS MLV INSLEY IOZ0d'Wd ce i WOOdOTHOVUE NVIUNTIS dd INEHdOTEAL— HOdSGNOLIMIWH=NWA NNGd 1099S \ SNOLLOQTI09 D190 TVHENILIS F aTLage WWval Wie a 706! AMLSNGNI SNINIS Nee NVIHOWHLVE SATA » eee as a SAT ANOE 9 HOHE SVCINOIN| XSOTOLNOAD Tvd 2 New York State Museum 1892—1909 Bulletins and memoirs. ArT THAT BS iE Hh 2S tS a a pie ere } * oo Seen? = Une ere 7: Koel S| SIXTH REPORT OF THE DIRECTOR 1909 71 meet 27 Glacial Waters in Central New York. By H. L. Fairchild. 64p. 27pl. Contents: . Introduction General description; preliminary outline Detailed description Batavia to Genesee valley Genesee valley to Irondequoit valley Irondequoit valley to the Ca- yuga depression Cayuga depression: Clyde channels Jordan-Skaneateles meridian to Syracuse Marcellus channels: Lake War- ren escape Birth of Niagara Falls and Lake Erie Onondaga valley to Limestone ‘valley I5 maps. Limestone valley to Chitte- nango valley Chittenango valley to Oneida valley Deltas Principles in delta construc- tion Description Theoretic mary Oscillations of the ice Warren waters Warren outflow Lake Dana Theoretic lake succession Description of the maps of glacial lake succession Summary of the glacial drainage history Bibliography Index succession: sum- front 5 No. 132 The Mining and Quarry Industry of New York State. By D. H. Newland. o8p. | Contents: Mineral paint Preface Mineral waters Introduction Natural gas Mineral Production in New Peat York Petroleum Cement Pyrite Clay Salt Production of clay materials Sand and gravel. Henry LricH- Manufacture of building brick ae : Other clay materials a -lime brick | Pottery Slate Crude clay Stone. HENRY LEIGHTON Emery Production of stone Feldspar Granite Bacnet Limestone : Marble Eo enite Sandstone Gypsum Trap Iron ore aaa Millstones Index 72 NEW YORK STATE MUSEUM Paleontology No. 128 Geology of the Geneva-Ovid Quadrangles. By Dp. Dana Luther 44p- @rrekets Food pests House ants Cockroaches Larder beetle Cheese skipper Cereal and seed pests Fumigation with hydrocyanic acid gas Index ee SIXTH REPORT OF THE DIRECTOR Igog 73 8 No. 134 Report of the State Entomologist for the fiscal year ending September 30, 1908. 208p. 17pl. Contents: Miscellaneous Introduction Injurious insects Poplar sawfly Grape blossom midge Gladioli aphid Green cockroach Typhoid or house fly and dis- ease Notes for the year Fruit tree insects Small fruit insects Shade tree insects ‘Publications of the Entomolo- gist Additions to collections Appendix A: Studies of Aquatic Insects. J. G. NEEDHAM Appendix B: Catalogue of the Described Scolytidae of Amer- Leet Ongt mOnneVlexicomer 1 lie SWAINE Explanation of plates Index Botany 9 No. 131 Report of the State Botanist for the fiscal year ending September 30, 1908. 202p. 4pl. Contents: Introduction Plants added to the herbarium Contributors and their contribu- tions . Species not before reported Gallus bankiva Analytical summary Relationships Addenda [Explanation of plates ne |, New extralimital species of fungi New York species of Lentinus New York species of Entoloma List of species and varieties of funeoiedeseriped, by C:. Peck Explanation of plates Remarks and observations Index Zoology feo. £20 Osteology of Birds. By R. W. Shufeldt. 382p. 26pl. Contents: Anseres Accipitres Anatinae Preface Modification of the larynx and Introduction trachea Cathartidae Appendicular skeleton Falconidae Anserinae Osteological characters synop- Trunk skeleton of the Anse- tically arranged rinae Relationships Cygninae eidenda Notes on fossil Anseres emanation of plates Remarks on the classification PalGnae of the North American An- seres Affinities Explanation of plates Coccystes glandarius Bibliography Index 74 NEW YORK STATE MUSEUM Archeology 1m No. 125 Myths and Legends of the New York State Iroquois. By Harriet Maxwell Converse. Edited and annotated by Arthur Caswell Parker. 196p. 11pl. Contents: Pt 3 Miscellaneous papers. Har- RiET MAXWELL CONVERSE Neh Ho-noh-tci-noh-gah, the Guardians of the Little Waters, a Seneca Medicine Society. Prefatory note Introduction : Biography of Harriet Maxwell Converse A. C. PARKER Pt « Iroquois Myths and Le- Appendix A. Origin of Good and gends. Harriet MAXWELL Con- Evil. Appendix B. The Stone Giants VERSE Appendix C. The De-o-ha-ko Pt 2 Myths and Legends. Har- Appendix D. The Legendary riet Maxwell Converse (Re- Origin of Wampum vised from rough drafts) Index Geological maps 12 Remsen Quadrangle 13 Geneva-Ovid Quadrangles IN PRESS Memoirs 14 Birds of New York, volume 1 15 Calcites of New York Bulletins Geology 16 Geology of the Port Leyden Quadrangle 17 Geology of the Thousand Island Region 18 Geology of the Auburn-Genoa Quadrangles 19 Geology of the Elizabethtown and Port Henry Quadrangles ‘Entomology 20 Report of the State Entomologist for the fiscal year ending September 30, 1909 | Botany 21 Report of the State Botanist for the fiscal year ending Sep- tember 30, 1909 SIXTH REPORT OF THE DIRECTOR 1909 Vill Peer THE SCIENCE DIVISION. AND STATE MUSEUM 7 The members of the staff, permanent and temporary, of this division as at present constituted are: ADMINISTRATION John M. Clarke, Director Jacob Van Deloo, Director's clerk GEOLOGY AND PALEONTOLOGY John M. Clarke, State Geologist and Paleontologist David H. Newland, Assistant State Geologist Rudolf Ruedemann Ph.D., Assistant State Paleontologist C. A. Hartnagel B.S. M.A., Assistant in Geology Henry Leighton, Assistant in Economic Geology D. Dana Luther, Field Geologist Herbert P. Whitlock C.E., Mineralogist George S. Barkentin, Draftsman Joseph Morje, First clerk H. C. Wardell, Preparator Paul E. Reynolds, Stenographer Martin Sheehy, Machinist Joseph Bylancik, Page Temporary assistants Areal geology Prof. H. P. Cushing, Adelbert College Prof. J. F. Kemp, Columbia University _ Dr C. P. Berkey, Columbia University Prof. C. E. Gordon, Massachusetts Agricultural College G. H. Hudson, Plattsburg State Normal School Prof. W. J. Miller, Hamilton College Prof. H. O. Whitnall, Colgate University Burton W. Clark, Washington, D. C. Geographic geology Prof. Herman L. Fairchild, Rochester University Paleontology Edwin Kirk, Columbia University 76 : NEW YORK STATE MUSEUM BOTANY Charles H. Peck M.A., State Botanist Stewart H. Burnham, Assistant, Glens Falls ENTOMOLOGY Ephraim P. Felt B.S. D.Sc., State Entomologist D. B. Young, Assistant State Entomologist Fanny T. Hartman, Assistant | Anna M. Tolhurst, Stenographer J. Shafer Bartlett, Clerk ZOOLOGY Frank H. Ward, Zoologist Alfred J. Klein, Taxidermist Temporary assistants E. Howard Eaton, Canandaigua Dr H. A. Pilsbury, Philadelphia Prof. Philip F. Schneider, Syracuse ARCHEOLOGY Arthur C. Parker, Archeologist Temporary assistant EK. R. Burmaster, Irving IX ACCESSIONS ECONOMIC GEOLOGY Collection Assistant in Economic Geology Gypsum, Akron 5m a ene aes t pace sa. s Uhlos each eee ey amit lltars eee ele 2a ee ae eal asad a * Glockwille yea eer Se SO has Ba ice eons ee (z2hig) 01 bin nates P48 anes a7 leet en een eRe ye re em AR ATE i; Vanes wiles. Sy ite ce. ei ea a. terse cece eeiahe cbse 9 en x LBa ge lcoig Manne nan, hee Daten ree a nerneE Cay VaR AG o MartisGo: Alem tag btie o oeee er oc he aon em aac bd ee Oak tne hells Scheer ei Se ee sie eta ease a Re eee oe) Net es : Pie lips oe oh Biel ee ote hak Oats aces ec hea a at's a 5 Victor: cc cee ori Wate repetcr tr, Rte atonal aa: Se ear ce ana, Oe } SIXTH REPORT OF THE DIRECTOR 1909 MMEETM I IGOOUCES 60. Shae Se ie de baw e een evade ccuntenes Pemmesmumerassociated With SyPpSUM.......... ccc eee eee cece enc swecens Clarke, John M. Demmmremeiicrwdalen Islands, Quebec. .... 6.26... cl ect eeccsce cece ee enes PALEONTOLOGY Donation His excellency Governor and Mrs Allardyce. Falkland Islands The following fossils and minerals from Falkland Islands ELS TILES GRRE ESE SIRI enn a I RRNTIE ESM Sit Git rey. cls, WMG asics eeesess, c,d io din cad awd we veil eae Glico els oi 8 ee er aie a oh io Lino Rvs Mae See dace een wee eS Mansuy, H. Hanoi (Tonkin) Indo-China Spirifer tonkinensis. Lower Devonic from Ban Lan, French China.. ee ee uc als nob. gud ope oa aceS swe oncas Schuchert, Prof. Charles Peemelireseimoen: Point Levis, P.O. Canada.......0... ccc ce we ees Maameantes irom Anticosti island, P. O.,Canada...........0.....00005 von Koenen, Prof. Dr A. Gottingen, Germany. Devonic fossils from Martenberg and Enkeberg, Germany From Martenberg, Germany (TEINS LAY CCTUSTIPE CSTE ee Aaa Pe SMMEMICORSIAMS Var: expansus VGN. .......6sccenccocererecssceruceees MME SCGE NOCOSUS. 65.50. cele cco gndels evldcaccdaeseascvawenced Summeegsians vor, Obliquus Whith. 0.060555. cece cee ecw e eee enees EES ECSeGHITTOrmis FOl2..... 0c. ace vc deg ses ucucddecesecees I ISU UICHINTOUMIC << a0. ca sv oacelsiced svg ues ceeacdsiesscevece'’s Sy EESTI RT na ee MMe TIME LI GL 5. o's ind a viva iow w dled’os ine oe ace ews wlde ea Vou INE BME GALA cas wo oid lcs os Geren erlovew Gc awlde'e clo eceecaescaee PE OMNES ISDE 6.5. spsc;0ladeie op sdjeie Daicis ass ovelde se sevelately's sv 'senee cues RANE ME SIS CAO et See asda abies ee ayia cae acess ed wnla's wok From Enkeberg PEESIUNEINIS VIUISICT Coc oc ee vice ene eb uc sae ecevueeceaee MEME EP MCUMIplexl SO00.. 0.6 cc ki eee eta e men ecceetnedanes UIE at 8 2 ks eee fin gv ced ec bedi ecssveeds Mueeen iets SMbIUSITOTING I/Cd. 26s... cece c sec cet cece ccc eee ceucseee EE GTS) SO lle ok bc nb ove de ces e des cbecbuedeks Bummmernmats war. atava Pech. 2. icc... cee ee cc ence ecu nseeeeuuevce Smmemrenrtis coy. cllipticuim Wed... 6c. sc cec ects cen se asessbeneens Memeo ts Anemstisellatum Wed... cc vec c cece clu ce ce seeelucdsleoees IMME ES 067M) tie Ws oo oe Sk. Ca Hx 0% ied bootie S bID 4 a8 od aa eraaueniaes ReetretaS LOtundodorsatiom Weds... ccc. ccc eins cede wnlncddseetwens IPE ia Cra PS SLL, Loar be ares od Gane tae Ala Wilson, John D. Syracuse, N. Y. MEET IS OIT OLOKIE Coa) ss aie's disc sidle'a'e'd 00 eves sia sioe dle Qevaieulbewes 77 Sw RDA HB HW ae Re AR 78 NEW YORK STATE MUSEUM Purchase Wilson, John D. Syracuse, N. Y. Tully limestone Brachiopods. artic Sith rec eee ae Note eid ie ee re GastropOdgrs< iit actin Se sue ee Chee one eves Saletan I Cephalopodss7oceends oo oo ae rae oe Sree es ee Hamilton : Corals nen a chet s bbs Ts Lave eae 6 Brachtopods (cz pic 6 Son dk se doe ot bees Ae en 16 Gastropods: ois s oie oie ds cos oa oa eek oo Eee ae ee 27 Tamme Vitalie MiGitars se pute eae eee “ye phae bls bole’ o cade oie ee ae 38 Gephalopods sis 2.52 were. cee ee ore eee ee to c 2 PrtlODItes yy ois yk ade ww «so coitus laced tice Oe Clorek i ete aieaten eae 10 Agoniatite limestone | Brachiopods. ... 65 605.60 le sss ossicles ore share cine terete) 2 oe 10 Cephalopods ci 0.2 jc cae sae sown ss lerstdanoi oko n gale Gta Men ieee Sy Onondaga limestone Gastropods) ois 60s 2 Soho sd Hong see nd 2 See ee 27 Cephalopods (Jo. 3. cein ee bois Ou on, 5 cent eee ee 3 Trilobites: 20).% cic. o3-s%ee onc coe ee ee ee ae ee Seu Cambric Trilobites s..050h0 20s oa eres aa eee ee 2 Lotal cen. os oie cee we» Sues eet sole oe oe ae Se oe Ze Collection Assistant State Paleontologist. Graptolites from Lower Siluric shales:.of Saratoga county .0...2.cce6. ood) tice oe eee 216 Clarke, John M. 3 Carboniferous fossils, Magdalen Islands, Quebec................. bbls. 4 Geological specimens, Magdalen Islands, Quebec...................--- 50 Cushing, Prof. H. P., Ruedemann, R. & Miller, Prof. W. J. Fossils, mostly trilobites, from the Saratogan (Hoyt’s quarry), Saratoga CO eee sath oes es hk Tiaie we Heel AW Bei ie Scola hart Le 400 Fossils from Beekmantown limestone of Mohawk valley.............. 25 Fossils from, Trenton limestone, Satatoga co... -...i...-25 06 32 Hartnagel, C. A. Eurypterids from Bertie waterlime, Herkimer co. 30 Hartnagel, C. A. & Van Deloo, Jacob. Eurypterids from Bertie waterlime; sElerlimtien SCO. 2 faye . 2.2... ee eee Ambly conte: Port Dar wan oom sts wyseae ort ee cine eee 2 hw Angilesite on’ cerussite,; Broken Hull IN. S.-W .-5 - ee oe ee eee Cabrerite, . Lauriumy; “Greece... 23 coset oe | Peck Ho C.= Albany, Loisite.: ‘Chester, s Nass. ae ae ee eae come 1 Gare eee Octahedrite, Somerville; Mass... .c0 cccd ees ce hee olde Purchase Comptoir Mineralogique Suisse, Geneva, Switz. Phenacite, San Miguel do Piracicava, Minas Geraes, Brazil Hodge, R. 8S. Antwerp Millerite. on hematite, Antwerp sicc.o. ace ese tee eo ee eee Elematite “Cbottyoidal).; Antwerp. 23s. ccs: + eee eee Hematite (specular) on quartz, Antwerp... yo. <2 aoa eee Hematite (stalactitic), Antwetpe.v2. 1.057 -5 35 0 ae ee eee Chalcopyrite on quartz, Antwerp..:......0...4... Lhe ee lee Pyrite ‘and: caleite,, Antwerp icc kd) stice es ok oe ee Pyrite and ankerite, “Antwerp oon) 22. aa edness ee ee Calcite ‘on ‘hematite, Amtwerpacsaes sone ee ee Calcite: and ‘dolomite, Antwetp 1.20.0 othe oe eee Caleite,on*chalcodite (large), Antwerpuw..s2.. es. 22. een eee Dolomite and ankerite, “Antwerp-s..i. son oes 2 oe oe eee ee Dolomite=(stalactitic),- Antwerp: c®..:<8.4 esc so eee Ankerite“on hematite, -Amtwerpi. occ hos inde: soe en Ankerite . (stalactitic),., Amtwerp ocr ay eee cei: Quartz & chalcedony, ‘ILoc.7 tinsee: Quatiz. Carve) oer tiles keene Wivianite wlocn cane a. nuee anno nme ae eeoscecece ees eee eee Oe eee eee eee ee ee eo eoeeoeees cee ee eee eee ee ee oOo ee ee ee eo (0 8 14 0 Pomphopoea” Saya ecepume wes blister beetle, adults on rose, June 28 . Niles, T. F. State Department of Agriculture Epicauta ? punc- ticollis Mann., blister beetle, adults, from Chatham, July 24 ° Norris, E. B. Sodus. Disonycha*pennsylvanica Ml, adult on apple trees, March 31 Zabriskie, George: Nissequogue, St James, LL. I. Galerueema luteola Mulls elm® leat beetle, larvae on, elm i july Forest, Fish & Game Commission. Same as preceding, from Green- port, July 8 Fish, J. H. Greenport. Same as preceding, July 14 Delafield, Mrs Albert. Greenport. Larvae and pupae of preceding, August 18 McKensie, P. B. Northport. Same as preceding, July 23 VanClefe, John O. Oakdale. Same as preceding, July 26 White, E. M. Sag Harbor. Same as preceding, August 5 Simpson, C. L. Amsterdam. Same as preceding, August 24 Miller, Mrs W. S. Boonville. Trichits een a sik sacs AOR eee ee Ae prom atiar) Lan.) sSpeeet saGe 36h vaccines qetae ie oe Hewett mrcula ta“ Mullen speens. cca Aan ee Bulimrou s°s p 6€¢ eS) Spe. o2s).ch ehhh oe eee Archachetina camierunens1s = (dAully)s spee see Rumina decoll a ta, eChinnae (speck sence eee Plaino rbis ‘corpenus- Giinns) “spec a. ce eee Ampubaria’: Co ru oat a Swains. “Spec... eee AL Sta SC altar seta Spec. sear IAS ae setae ete ch Pi Ai eee Paludina lecyt hordes” Benson spec... 2 stat ial ee Adamsiella variabilis) (@Xdamis)). = Spec] °) jee sae Lucidella+rva ures la ero spec. in. eee eee Hedi c ina se 0. sta ta. “Gray, sspee ac. sa. ie eae eee ee Fem ayo fe Gray,, Specs ates ce ale eae ey eae eee Celera hon ene Ao meritel ba: Lam) specexus oon ites cae ee Purchase Mammals Elliott, Joseph. Beaver River Porcupine, Erethizon dorsatus Gena: SiktiniS:; 25: eee Klein, A. J. Albany Gray fox, Urocyon cinereoargenteus (Schreber) esi Ward’s Natural Science Establishment. Rochester Moose, Alces ‘americanus Jardine, group) -of “imommred SPECINVENS 5h ae eee Ga aiealle ae ab Sec Shc, che a gies ares aes Acker, C. F. Conesus Lake Double-crested cormorant Rhalacroconax aitniuus a @lcss: ) mounted Specimen. 7s ficio ok es Pde eee eee ee eo ee Gowie, W. D. East Greenbush American bittern, Botaurus lentiginosus (Montag.), Cio bs ere nA Rraee ter Mt EUR B Ce Page 5h ane lF Lara incin o> White, Peter. Albany Short-eared owl, Asio fla miure ins (Pomtop), skin... ae Fish Sea robin; “P’rion.ot ws (ca poli nis inn) ys ieCun sae HH ND HH HH He NAR PB HH DY HWW HDKFH HY HY NDNA RM __ Sti REPCRT OF THE DIRECTOR IQOQ Collection Mammals Semsimiaee deer, Odocoileus virginanus borealis Miller, 55 rb Sg Re Ue emotes ylvilagus transitionalis (Bangs), skins.... Mit see ee tiizon dorsatus (Linn.), skin......0....0.. Emenee Nis norvegicus Erxleben, skins................4. Pmnennce Aactomys monax (Linn.), skins................ mente I aimias striata lysteri (Rich.). skins.......... mmonremole Scallops aquaticus (Linn.), skin.......... meebrown bat, Vespertilio fuscus Beauvois, skin...... meee Aris borealis (Miller), skins.........0.....0. Birds Meron, bo WtOtrides virescens (Linn.), skin............ emer eOolaptes auratus luteus Bangs, skin.............., reo tyiis brachyrhynchos Brehm, skin............... Prmmonomeamius vuileparis Linn., skin... ......000 5.0000 es bees eeneeeeeominis linaria (CLlinn.);. skins:......6s.00.0600.000. mmenean coldinch, Astragalinus tristis (Linn.), skin..... Poa primis pinius (Wilson), skin. ......0... 0.00. ..5.05-- meeeepictow, spizella monticola(Gmel.), skin........0....4 mmepige spatrow, Spizella passerina -(Bechs.), skin........ eme-colored junco, Junco hyemalis (Linn.), skin.............. Meeeeevarpicr Dendroica coronata (Linn.), skin.......... Back -poll watbler, Dendroica striata (Forst.), skin......... _orinich Mendroica vigorsii (Aud), skin......../....... Beewn creeper, Certhia familiaris' americana (Bonap.), ey eck cre 8 Sia e ge ches Goole URSA Re eis os ole dunce ees Semeen-crowned kinclet, Regulus satrapa Licht., skins........-. Mumeenacked fhtush, Hylocichla ustulata swainsonti I oe ee Se, Pelee cha SY ihe do ga aoa Wale wale aa DRL mem thrush, Hylocichla guttata palasii (Cab.), skin. Fishes Mmtertpomotis gibbosus (Linn.), spec.............00-- meee ned tlavesce@ns (Mitchill), spec.......... 05.0000 08s Mr sGaiis crysoleucas: (Mitchill), spec-...........056: Reptiles Ring-necked snake, Diadophis punctatus (Linn.), spec....... mumemstiake, Natrix sipedon, (Linn.), spec.........ccecesceeee Semersenake TLhamnophis sirtalis (Linn.), spec........... Meee turtle, Chelydra serpentina (Linn.), spec......... Painted turtle, Chrysemys picta (Schneider), spec..........:. mpotted tortoise, Clemmys guttata (Schneider), spec.......... YS DO we AbD bh UI A BD Ft re at Ce A ee A oe Lon NO FW H WH A 94 NEW YORK STATE MUSEUM Batrachians Spring peeper, Hyla-pickerimei1 Ciolbrook), Spec--. =. eeee Tree toad, Hyla- versicolor le Conte, spec... eee Bullfros, Rana catesberana shaw, Spee... nde se ee 3 2 Wood. frog, Rana. sylyvativea Le Conte-spec:- 2. -.. ee a I ARCHEOLOGY Collection Burmaster, E. R. Port Jervis site Jesuit rime oS 6 ees k fe See oes oe eee TfOM TINGS W060. hes Fis bes ae de oe De eee Pewter ring; glass setting +. tiene ae ee ee oe Bronze. sp00m.>. sis oy 0 8 ee eee ee String small brass beads) 725). Se.8G cae see ee oe String large avhtter beads tis ae se eee ee ree 20 4c) pee eee String small white beadsy%-s.5 sie) eras on oe ee String blue glass and amber beads] ..22 >.) 62 eee Moorish ‘beads... 2.2.2 /20 Gee eee ete ee Shell worgets = foe fan a oleae = a ; Preserved fabric, fragcment:. 7.40 at. 2 ok ee ee eee “R LDippet’ pipet Sit wcrac B. oe ae eee eee 2 arm bands ct coppers. 52.28 2 eee ee eee Skeletons, parts of; including skulls... 7.0 -4:40. 9. .c2. ) 0. ee ey Brass- buttons 255) st00 ie 5 Hie eee ee El awik sabes! 205 72 nares eee A eo. Sa Bronze™bell- 2.2. vk ee eee Juels 24.05 ee Iroquois: pipes 25. ee 550s pe ee ee Pipe bow] 3220 .ee nase eee Parker, A. C. Gotget; broken? ec Se re ee Atrowheads: 2.5.05 \eee aoe 1 ak coe os ee ee Celt 5 68 Sse aa i eae ee tie eee ce Brass; worked: 1 raciientst-s ce aa te ee «nh he athe e baat See Rude stone axes: Akula eee ease eae eee te ie Pie Luther, D. D. Naples. From graves on Canandaigua lake Rheolite ‘Knitte ieee eee ere ce ep oe a oe Stone tubes: 2005550 ie a ee ee pe ce Se Native copper ‘chisel p35 se eee ne ee 2 ee ee Strings of shell beads ....... Rue tiple: Sa Pipe eck aS Si oe ee eae ce Exchange American Museum of Natural History. New York Bannerstone, “Ulster cO:.2s). ned whee ee nee Bannerstene, Philipstowinvenc.ccees soc Sew ae ee hee eee eee 30 He NN ABW A — ee es ee ee eee ee eS eee ee ee ee —— ee Ee SIXTH REPORT OF THE DIRECTOR IgGOQ \O Cy MIRE VAT CON 5 se te oe ee ee ee eee eee ee enew rene Sepeee (te ole broken) Tuthill township, Ulster co.................. Gorget (2 holes, broken) Grinnell, New Hamburg, Dutchess co..... MME EY CSECIICSLCL COL. i. cece eect e ee eee eb eeeeanane meme eine ston, Ulster CO... ... 0... 6c cee ee cece sees sees Summertime odicertics, UISter CO... 6. etc cece cece cece eeeees Sepeeeeeaeze Indian Brook, Philipstown.............0cceee cece cea’ eMart censacik, MWUtChess CO... 2... eee lee we eee eee nee RemmmEemaT ASIN, A NTLIPSCOWN. 5... eee ee te tree cece sees RE Ee ISECE CO... cece ee ie he cee ete e ea adaeesceus Bemmeremaceranse, Dutchess: CO... 2... ee ee eee bee ee Gera ee SR eee eockport, Coltimbia cO.......-.......65 RENT eth per ert ne eumencromessatcerties, Ulster co... cc... lee eee case eee tebeees a Pe Lois we nine ols eee G'S dv ale Oe ede blb ewe we MMe SSO MSW ISECT COL ais i cicc cece cee cee lew cece sean ce eevee’ 5 EST CTS RS Se a TMG SUOW IL... cess eels ke sy c cee ws dasa ee ees ecuaedases i SEFES iy SSS SEES Scie ar te ea I On HHM DN AH HH HB Ye Re YR a ETHNOLOGY Purchase and collection Parker, A. C. mmmmcmcwmene Grand River, Ont... .....06. 0000 cde ce cece ea eens Meinmrogedancina uses Olly... 2... 0... ee eee ese cect cnees iermelub, carved with symbols of clans............... a eee oS path eh MMMPEIREM A SeGrPISICI, “SCL OL. cine ce oe nse ete eels ole taa eee aes Mmmishea 20ura tattles, to ShOw ProceSS..........2.. ceca eet eccceane mumeiiecaid to have been worn by Red Jacket...............cc00ec008 Se PUTER ERs RN ee teary? WP ab avn ae EE te on ee od caleba Doge de aveadens I ete Foe oo sake ici nine aie docu AOvidid sioawen sc bgec ey ¥es I PS eal ese 2 ot cecchs cio w ace ei Khe wd alee vice Vvicie wie tle es ME MP re Sissi ote la dies sine pee ie a e’alad bas ue bebe 8 SR Ces Ss oe Ge ave ola sie c es sa ove gels ob desic te eee SE CHISOM OM, SETING. . ob. a ce ee ee eae es S Suit Spe Oa oe emmmmisseiiitsitatine Setieca fraditious..... 051... 0c ete ce b ee cence RII rs eet err SG A Casas se we ve vac uea bes NE eA sc Se IE. oc wd e's be ale ee sleacacvlaveceves EPI nL Lan lola de bof ncin eats wld Cove Ve eevee cee NN foes 2 cde sh cisiecs cops Goce be ced bile peeewoveve IES ears Ns bg Gee ci hiidsc sche che bcp eeed ees esceebecs Corn baskets, series used for planting, harvesting and sifting......... NEMEC so oe a. wie Se ss eee neces as @decncdeccacecscuuse False face CoS eee ee eee et bel (We ono oe taba eoesereeeseeseeeseereeer ees eeseeeeoeeeoee ees eeeseese eee eseeeeee288 8 eesrereese eee sess eee ee eeee ee eeeeeere eee ees e ee ee ee ee eeeoee Bark barrel made of elm bark Bark barrel, birch AH AR weH NY A A Sse eens Iwas ee Oe) eM 8 (es 18 ).6) ee leke 18 6) (¢ (61 6) 6 9 (6 6) 6l\e 6.8 6 6; 0 ©, Op 6, 6).6).0) ene) «85 96 NEW YORK STATE MUSEUM Algonqjtin birch bark canoes: .20ks.cees 6 ks). oy eee I Paddles 3 .eEi 00h. Jeon eae tee eta ee 2 Indian ‘corn on. Strings; varietiess. a.) - ohn eee ee eee 5 Indian bread ys s.2 saad ceew diy ame Cod nde Sen I Paddles carved. with: figurines #2) gx. 25.) se eee I Baby moccasins,..pair x05 .:1o han oe ad eae es Ue Sone ae ee r Burden strap; woven ‘of elm bark y.-.n2.5 nee ore Dee I Muskrat pelt stretcher. iin iv: eis fee oe ee eee I Bark “rattle “Ceci cock ee eee Walovasoavete ah acevo ee See I Burmaster, E. R. Seneca brooches... 56s. ss ae shee eeeius 6 cae eee ee Purchase Schmid, A. A. Albany rstring of Dutch roanokewampuniy. ........sseen so ee eee REET So Beaded: bag ry... 5 a ee ae ie ee aie I speck, D7 BP. G:.) Pinladel pina, Ra, ; Huron: toy bows. a. Gibie etd a eg Mhecte ey ald Bb ed’ etd e058 iy. toe tO eres ar I ELUuron Spoons: os awie eos. once ieee ee ate a 3 Dolls as hh PR Sc Bemata Haas Wid ale POS LETS Oo es) EAE ee cee Zz Beaded: pockets... Sav ehh is ee adores o cudtodl eae ie eee 2 mmowshoe, (ee dle rs..cie are tose potent epee etal eer ee te if Snowshoe \punch.c she hea) eee eee oe eee eee eer pares bie a 3 Donation Alexander, C. P. Fonda Pottery, “fragments: Jn \.\. 3 os sss sieseree d seers paterson cee 10 WEF OW 2 POIMbS Msi) vig oF @ aiein'e a ternin aaialitencoeleveie eens etesiy oa elleae «eae eee 5 Hutchinson, Hon. Frank. Albany Potsherds 0% (oo n0 Slo. d s Bee Vi ae a eo ee 20 Animal bOmes 3 8 ck ess Rois be lok Sa Ue BOOn TR ne eee 25 Pipe | bow!) vo. S00 Ae oie oa SEs es BA ee ee ee I Lee, E. Gordon. Canandaigua Large adzlikescelt, fime Specimetl... 4....22-55-0--. 1+ he ee I 327 SIXTH REPORT OF THE DIRECTOR 1909 97 pee RELATIONS.OF THE LITTLE FALLS DOLO- fee (OALCIFEROUS) OF THE MOHAWK VALLEY Rbk ULRICH ANDi. PP. CUSHING Introduction _ Ina recent paper Cushing made the following statement about the Little Falls dolomite :* In the correlation table on a previous page the Little Falls dolo- mite (the local name of the supposed Beekmantown of the Mo- hawk valley) is given as the equivalent of division A of the Cham- plain valley and of the Theresa formation of the Watertown region. It should be frankly stated at the outset that this is the element in the table whose precise position and relationship is quite uncer- tain. . . Ulrich’s discovery of the unconformity between divi- sions A and B in the Champlain valley, necessitating the separation of division A from the Beekmantown formation, at once raised the question as to whether the entire Little Falls dolomite may not lie below the horizon of the unconformity and hence not be Beek- mantown at all, but be properly correlated with division A and the Theresa formation and possibly even with the Potsdam. . . There is a second doubtful matter connected with the Little Falls dolomite, namely, whether or not it is a single formation. Vanuxem carefully distinguished the upper portion of the formation, the so called “ fucoidal layers,” from the remainder, and he has been followed in this by most other observers in the district. . . either the bulk of the Little Falls dolomite is of substantially the same age or else is an undiscovered unconformity between it and the fucoidal ayers. During the summer of 1909 an effort was made to gain the information whose lack was indicated by the quotation above. Cushing and Ruedemann made a careful, detailed study of the section about Saratoga, following which Ulrich was shown over the section. Thereafter Ulrich and Cushing studied a series of sections, commencing at Ticonderoga in the Champlain valley, passing south to the Mohawk and thence west to Little Falls and Newport. In much of this work Ruedemann also participated. In the following account of the results of the work, the bulk of the paper has been written by Cushing, with an occasional comment or insertion by Ulrich. The section on the “ Strati- graphic position of the Potsdam, Little Falls and Tribes Hill *Mr Ulrich’s contribution to this paper is published with the con- sent of the Director of the United States Geological Survey. *Geol. Soc. Am. Bul. 19:174. 98 NEW YORK STATE MUSEUM formations’ was written by Ulrich, and the final chapter on oscillations is a joint production. The section. The rocks with which this paper is especially concerned are those heretofore classed as Potsdam and Beek- mantown (Calciferous). At Ticonderoga we found the ordinary Champlain succession of these rocks, Potsdam sandstone, grad- ing up into division A of the Beekmantown through a series of passage beds, and this followed by the other four divisions of the Beekmantown, as established by Brainerd and Seely. The Potsdam is chiefly a vitreous, well cemented, light colored sand- stone, with some weaker beds with calcareous cement in the upper portion. The passage beds consist of alternating beds of vitreous sandstone, calcareous sandstone, and gray dolomites which are usually somewhat sandy. With disappearance of the sandstone beds we pass into division A, chiefly a dolomite forma- tion, largely of dark gray, finely crystalline beds below, running up into more coarsely crystalline, very light gray beds above, which are apt to be full of chert. Though not positive in the matter we are disposed to believe that Brainerd and Seely te- garded the latter as forming the lower portion of their division B. At all events we find an unconformity at their summit wherever we have seen the horizon exposed, and we class them with the darker colored dolomites beneath. Frequent reefs of Cryptozoon, chiefly C. proliferum, are found in both the dark and light colored parts of the formation, and the summit is very apt to be formed of a massive, Cryptozoon reef, often heavily silicified. Lying on these in the section we measured at Ticonderoga appear beds which seem to belong to division C. The beds of dove limestone which constitute the most distinctive part of division B at Shoreham, Vt. and elsewhere in the Cham- plain valley are absent in the Ticonderoga section, apparently because of nondeposition. Division C is followed in order by the beds of D and E, and the last by lower Trenton, but the seme. cession is somewhat disturbed by faulting. Our section at Whitehall exhibited the Potsdam, passage beds and overlying dolomites, reaching up into the coarse, light col- ored, upper beds, but the summit and the overlying beds were not reached. What was seen was exceedingly like the corres- ponding part of the Ticonderoga section. : Again at Saratoga the section was quite similar, though with two prominent differences. Instead of the Potsdam grading SIXTH REPORT OF THE DIRECTOR 1909 99 upward through passage beds into dolomite, the passage beds were between it and limestone, which was, in turn, followed by dolomite. This is the limestone from which Walcott obtained the Saratogan fauna which he described. It seems to us to bea calcareous phase of the lower portion of the dolomite formation. We are proposing for it the name “ Hoyt” limestone and regard it as merely a local member of the dolomite. The name “ Green- field” limestone, given to it by Clarke and Schuchert, was pre- occupied and must hence be replaced. At Saratoga also there is no trace whatever of the beds of the four upper divisions of Brainerd and Seely’s Beekmantown, B-E inclusive; instead the limestone heretofore called Trenton rests directly on the dolomite of division A. The Potsdam is thinner than at Whitehall and Ticonderoga, the loss being from the base. Passing from Saratoga to the Mohawk valley the Potsdam rapidly thins out to disappearance along with the passage beds, letting the dolomite down on the Precambric. The dolomite formation, however, remains substantially as before, and is over- laid by the more calcareous formation which Vanuxem called the meiceiga! beds. For these we propose the name “~ Tribes Hill” limestone, restricting the Little Falls dolomite to the beds beneath. The one overlies the other unconformably. The Tribes Hill thins westward and disappears west of Little Falls, letting the overlying Lowville limestone down on the dolomite. The general section then, as we interpret it, is as follows: i epee divisions of the Beekmantown; un- Beekmantown 3 named as yet | Tribes Hill limestone —_——— Unconformity Little Falls dolomite; Hoyt limestone as a local, basal phase Theresa formation; passage beds Potsdam sandstone Saratogan Historical ffs not intended here to give an exhaustive résumé of the literature which deals with the district, but merely to indicate some of the more important papers. IOO NEW YORK STATE MUSEUM Vanuxem, 1842.1. In reporting on the Calciferous group in the third district, Vanuxem distinguished three varieties of the rock: The first siliclous, compact, and perhaps a continuation of the Potsdam sandstone; the second a mixture of yellow sand and car- bonate of lime, in irregular layers, the mass from whence the name Calciferous sand rock was derived; and third a mixture of the Calciferous material, which is usually yellowish, and of compact limestone, containing also some slaty matter. The action of the weather gives these layers the appearance of a gothic fretwork. These materials are often coated over with a greenish shale; and the whole mass has been designated, in the annual report, by the name of Fucoidal layers. In the annual reports the fucoidal layers were separated from the Calciferous sand rock, in consequence of always observing that they were above the great mass of the latter rock; overlooking the fact, as it seemed to be of little importance, that the fucoidal layers were always covered by a few, or more, layers of the Calciferous rock. A reattention to the subject was caused by the observations of Dr Emmons in the second district, where the mass above the fucoidal layers is greater than the one below it; the combined observations of the two districts showing that the two constitute a group, in which the fucoidal layers are included, and therefore a subordinate mass. Fossils are rare in the Calciferous sand rock, but in the fucoidal layers there are many individuals, though the kinds are few. Most of them are peculiar to this rock: ; As a marked difference exists between the Calciferous sand rock and the fucoidal layers, though they form one group from the in- tercalation of the latter, they will be treated separately, from the rule which separates objects which are different. Comment. The above excerpts, given substantially in Van- -uxem’s own words, show plainly that- this excellent observer was so impressed with the differences between the two formations that he described them separately, and likely would not have classed. them together at all, except for the reported Seen- ditions in the second district, unfamiliar territory to him. He noted the differences in lithology and in the fossils, and also that the fucoidal layers thin out westward, being very thin -at Little Falls. Emmons, 1842.7 Emmons, in the second district, which in- cluded the entire east and north sides of the Adirondack region, found the Calciferous in greatest variety and in greatest thick-. ness. In the Champlain valley he included the lower Chazy in the Calciferous, and in the lower Black River region, the beds of “Geol. N.Y. 3d Dist pesonce: ? Geol. N&Y. 2d. Dist.sp. 05a: —— SIXTH REPORT OF THE DIRECTOR IQOQ IOI Stones River age, since separated as the Pamelia limestone. He attempted to recognize the fucoidal layers in his district, but states that they lie just above the Potsdam instead of occurring at the same horizon as along the Mohawk, and it is plain that the term, as he used it, referred to the passage beds of the Theresa formation, and not at all to the Tribes Hill limestone. Hall, 1847. In volume 1 of the Palaeontology, Hall describes and figures a few fossils from the Potsdam sandstone and the Calciferous sand rock. The Calciferous forms, with the excep- Memeor Lingulepis acuminata which is from the basal part, and of four species found loose, came from the upper part of the Little Falls dolomite and from the overlying, calcareous layers (Tribes Hill limestone) along the Mohawk. Hall, 1884.2 Describes Cryptozoon proliferum from the Calciferous of Saratoga county, with description of the genus. Walcott, 1879-91.* Ima series of publications Walcott refers the Potsdam sandstone to the Cambric, describes the fauna from the Hoyt limestone, and recognizes it as Cambric, though re- meee ade first to the Calcitferous. He regards the Hoyt limestone as a local, calcareous phase of the upper part of the mersdaim Sandstone and states that Lingulepis acu- minata ranges up into the Calciferous sand rock, and that a species of Ophileta ranges down into the Potsdam. He draws the line between the Cambric and Lower Siluric north of the Adirondacks between the Potsdam and the Calciferous sand rock; about Saratoga in the lower part of the dolomite above the horizon of the Hoyt limestone. Comment. Walcott’s work was, of course, a great advance over everything that had preceded. We differ from his conclusions chiefly in regarding the Hoyt limestone as on the horizon of the basal portion of the Calciferous rather than of the upper part of the Potsdam; in holding that substantially the same fauna characterizes the upper Potsdam, passage beds, and lower por- tion of the Calciferous; and in classing the whole of the Cal- ciferous of the Saratoga region and all of the Calciferous of the Mohawk valley, except the part here distinguished as the Tribes Hill limestone, with the Potsdam as Saratogan. 1 Op. cit. p.270. “N. Y. State Mus. 36th An. Rep’t Nat. Hist. pl.6, description. pm. Y. State Mus. 32d An. Rep’t. Science, 3:136-37. fee. Geol, Sur. Bul. 30, p. 21-22. >. Geol. Sur. Bul. 81, p. 205-7, 341-47, 363. LOZ NEW “YORK STATE MUSEUM Brainerd and Seely, 1890.1 In a most important paper Brain- erd and Seeley give results of the first careful and detailed study made of the Calciferous of the Champlain valley, disclosing its great thickness and its considerable fauna. They distinguish five subdivisions of the formation which they call divisions A-E, inclusive, and map several of the most important areas in detail. The work on the whole was well done and has formed the basis for all subsequent discussion of these rocks in the Champlain valley. Prosser and Cummings, 1896-1g00c.2. In two publications are given a series of carefully measured sections with discussion, from Trenton Falls on the west through the Mohawk valley to the Saratoga region on the east... The thickness»ot (meee Falls dolomite in the Mohawk valley was made known for the first time and, following Vanuxem, the fucoidal layers were care- fully distinguished from the dolomite beneath. Cleland, 1900-3. Announces discovery of an abundant fauna in the Mohawk valley Calciferous (fucoidal layers) which is de- scribed, and the horizon traced from Fort Hunter and Tribes Hill to Little Falls with collection of fossils at several points. Cushing, 1908.* Gives a general! description of the section in Jefferson county, describing the Theresa formation—a_ thin series of passage beds and following magnesian limestones — which directly overlies the Potsdam sandstone and is uncon- formably overlain by the Pamelia formation, of late Stones River age. The Theresa formation was so thin and so htholog- ically similar from base to summit, that it was not suspected that more than one formation was represented by it. This, how- ever, proves to be the case, as will be later shown. It is also argued in this paper that division A of the Beekmantown more properly belongs with the underlying passage beds and Pots- dam than with the purer limestones of the remainder of the Beek- mantown, and that with this readjustment the upper Cambric (Ozarkic) and the Lower Ordovicic are separated by an uncon- formity everywhere in northern New York. Purpose of this paper Our comparative study of the region has, we think, made clear the correlation of the Calciferous of the Champlain and Mohawk ~ 1Am Mus. Nat. Hist. Bul. 3:1. JN. .Y. State Geol: 25th An: 7 Repit-p.o1es50: INGE Y. State Vins buleeae Sontiaas de ailbes igi aio aeeoe “Geol. Soc.;Am: Bil 1ost55-76: SIXTH REPORT OF THE DIRECTOR I9Q09 103 valleys and seems to us also to show that the Little Falls dolo- mite (Division A and the lower part of B) does not properly belong with the Beekmantown, either structurally or faunally, and has been heretofore classed with it simply on the basis of supposed lithologic resemblance; that it is separated from the remainder of, or rather the true Beekmantown, by an uncon- formity, while it invariably grades into the Potsdam beneath through a series of passage beds; and that faunally also its asso- ciation is with the Potsdam, the Hoyt limestone of the Saratogan region being merely a more calcareous and more fossiliferous phase of its lower portion, of very local character, rather than a phase of the Potsdam. Detailed sections Commencing at Ticonderoga on Lake Champlain the sections will be given in order, passing to Whitehall, 20 miles south of Ticonderoga; to Saratoga, 35 miles farther and south-southwest from Whitehall; to Cranesville in the Mohawk valley, 20 miles southwest of Saratoga; and then west through the valley to Little Falls, Middleville and Newport, 35 to 45 miles away. Section at Ticonderoga Brainerd and Seely have mapped and discussed the Beekman- town section in the vicinity of Ticonderoga. It 1s but a few miles west of their type locality at Shoreham, and they map all five of their subdivisions of the formation. It may thus be re- garded as giving a quite typical representation of the Beekman- town section of the Champlain valley. Since our purpose was a detailed comparison of a portion of the section with sections elsewhere, we made no effort to study the whole in detail. Potsdam sandstone is exposed in the creek through the village, and commencing 60 feet above the creek level we measured the following section up the hill to the north, known as Mount Hope, the 60 foot gap probably consisting partly of Potsdam and partly of passage beds: SECTION JUST NORTH OF TICONDEROGA ; : Feet Inches 34 Light gray, finely crystalline limestone, to top of Res ys 5 ae Roo sis ge bsdevereuei Re esa ye ail 8 MEEeaAlearecous Sandstone. ..... 6. cote s wee veees ii *Am. Mus. Nat. Hist. Bul. Mega =e b 104 NEW YORK STATE MUSEUM 32 Blue gray dolomite; cross-bedded, rather coarse grained; frequent drusy cavities with calcite and quartz; very sandy midway with chert pebbles and flat; dine erained pebplesms. cise 31 Medium grained, gray, crystalline hmestone; many nodules of crystalline caleitevcemieal ly se ee 30 Hard, vitreous sandstone, irregular at base over the nodular surface of the limestone beneath.... 29 Gray, crystalline limestone, in four beds, finer srained toward top. 14 acter. 6 ee 28 Gray white sandstone, somewhat’ calcareous...... 27 Hard, vitreous, whitish sandstone, coarsely ripple- marked above. ch Hie ee ter ee eee 26 Gray crystalline limestone, with calcite nodules... 25 Alternations of thin, slaty limestone and thin seams of gray, magnesian limestone, much laminated. . 24 Upper half of gray dolomite, lower of dark gray, oolitic: limestones: Voss see. ee eee 23 Earthy, magnesian, rotten limestone, surface nodu- lar and of red:colot.. a. eee ‘ 22 Dark gray, oolitic, magnesian limestone, ovules weathering blackishix: .).c= ae eee ee 21 Fine grained blue limestone, weathering drab; earthy and somewhat laminar; upper 2 inches shaly and with nodular surface which weathers C20 Ae ete MEN Nn 2 onns Se, s SOse eS ce 20 Similar to that above; very uneven upper surface maith 1 ich to 2: inchessced, lamimareshalesas COvier 2: feet, Osnches t0ce san rae ee 19 Dark gray, oolitic, magnesian limestone, ovules weathermoriblackish: 15 2 .ihaca5 be poe seers 18 Blue, earthy, fine grained, somewhat laminar lime- Stones WieatMe RS uCralin. hs tepee. tants eee eee 17 Dark blue gray, crystalline, suboolitic limestone; upper surface is irregular and weathers red..... 16 Thin, sandy, blue limestone bands with shale part- ings, and one 4 inch seam of cross-bedded sand- stone; upper I foot very thin bedded, and red- dish: holds ine al ep is case Umainla tase. 15 Thin, irregular, shaly limestone, with fucoidal markings and ane i esos are) Waite are Feet: II ie Inches Io SIXTH REPORT OF THE DIRECTOR I909 I05 Feet Inches Stan, whitish, vitreous sandstone................ 10 13 Dark blue gray limestone, finely crystalline, heavy bedded, frequent grains of fine quartz sand..... 7. Matha, wilite, vitreous Sandstone..........:...... 2 3 11 Dark gray blue, calcareous sandstone, weathering Pe prayen, rotten Stone, especially above........ 4 4 10 Gray, finely crystalline, somewhat magnesian lime- stone, with occasional sand grains; thick bedded; Memcmesinrace ripple-matked.-..:........0...%. 9 & 9 Irregular parting of shaly limestone with fucoidal - oD RES. Sg Saal ie 2 8 Gray, subcrystalline limestone, with sparing quartz grains; lower portion laminated and mottled eeM I ee LITA ooo She a,c oie Gas hela eae evens we oan 2 7 Dark to light gray, subcrystalline, magnesian lime- stone; thick bedded; many rounded sand grains; Saemeenoatiics in upper portion............... 6 Gray, magnesian limestone hke that below....... I 8 IE te OM ins ke pk ee es I 8 4 Gray limestone like that beneath but lighter in TILES . 2 2 o sth ete ee eee eee re oe I 3 Fine grained, finely crystalline, gray, magnesian limestone, with fine, interrupted black lines; fu- coidal markings; sand grains abundant on upper mete Orimerwise Sparse... 22.5. eed ce ee eee 2 2 Shelly, laminar, calcareous sandstone, with streaks Bennie sandstone; iiccidal markings.......... 3 I Blue, crystalline limestone with occasional small, SURES OTAIIS. 13.7.0 6 ee css dee ee I 3 Peaeenenieistiess. See. eens Ree ee ee I12 8 This section is on the general horizon of the Hoyt limestone of the Saratoga section, though including somewhat more than that, both at top and bottom. It is also the same as the lower portion of the Whitehall section and shows the beds which are concealed there. A somewhat unusual feature of it is the dis- tance upward through which sandstone layers of Potsdam char- acters run. According to Brainerd and Seely’s map they re- garded the lower part of this section as belonging to division A and the upper to B. 105 NEW YORK STATE MUSEUM One mile to the east of this section is another which shows higher beds, an additional thickness of about 100 feet being ex- hibited. The section is exceedingly similar to that of the upper portion of the Litthe Falls dolomite at Saratoga, bluish @tay.e finely crystalline dolomite below, often with bad odor when freshly broken, with many nodules of crystalline calcite, often drusy, and with coarser grained, whitish, crystalline dolomite above, with much black chert; the section capped by a massive 6 foot reef of Cryptozoon, much of which is chert. Tints is direc, and unconformably overlaid by beds which seem to us to belong to division C; certainly they have the lithologic character of that division. These are followed in their turn, going north, by the beds of divisions D and E. ss Discussion. The bulk of this second section is mapped by Brainerd and Seely as belonging to division B. They describe the division as follows: , | Dove-colored limestone, intermingled with light gray dolomite, in massive beds; sometimes for a thickness of 12 to 15) tcemmme planes of stratification are discernible. In the lower beds, and in those just above the middle, the dolomite predominates; the middle and upper beds are nearly pure limestone.' We found no dove limestone in the section. Likely the light gray dolomite is that forming the upper part of our section, though if it be, we fail to understand the lack of mention of the chert which we find in it everywhere abundantly. In any case it is the same horizon which we find everywhere to characterize - the summit of the Little Falls dolomite. In this section it is, as we believe, in uncomformable contact with division C and this is followed by the whole of D and E, the two upper members of the Champlain Beekmantown.. Except where (croded@iana, during the time interval which followed, the summit of the Little Falls dolomite at Ticonderoga and elsewhere is usually a Cryptozoon reef, often heavily charged with chert, as is the case here. Section at Saratoga The Saratoga district 1s considerably faulted; glacial drift is widespread and often heavy, and a complete, detailed section can not be made out from study of the surface outcrops. The Mohawkian rocks rest on an uneven, eroded surface of the dolo- mite group, varying beds of each group being at the contact in the different exposures. The general section is as follows: Ope ction p22: SIXTIZ REPORT OF THE DIRECTOR IQOQ 107 Trenton limestone; with usually a small thickness of Black River limestone beneath Unconformity . Tittle Falls dolomite; light gray to dark gray, crystalline to subcrystalline dolomite, sharply bounded rhombs embedded in a cement which is more or less calcareous and dissolves away leaving surfaces of sandy appearance; certain layers are full of nodules of crystalline calcite, others are drusy and hold calcite and quartz crystals; black and gray cherts are frequent “meetiain morizons; a Cryptozoon reef occurs in the upper part of the formation in a dove limestone band; otherwise fos- sils are very scarce. Thickness at least 150 feet and possibly 200 feet Hoyt limestone member; blackish, subcrystalline, pure or only slightly magnesian limestone alternating with beds of blue and light gray dolomite; quartz sand grains in some of the beds, Increasing in amount below ; in the lower portion beds of calcareous sandstone and more rarely of quartzose sandstone; contains many beds of black oolite, most abundant near the base; con- tains Cryptozoon, trilobites, gastropods, and Lingulepis acuminata at many horizons. Thickness 80-120 feet Passage beds from the Hoyt limestone to the Potsdam sand- stone; alternating beds of hard, vitreous sandstone, gray, cal- careous sandstone, blue or gray, crystalline dolomites and magnesian limestones, and black, oolitic beds; contain trilo- Meseand Lingulepis acuminata. Thickness 40-60 feet Potsdam sandstone; light colored, vitreous sandstone, with occa- sional layers of calcareous sandstone in the upper portion, and more or less coarsely conglomeratic beds at base; thickness variable because of overlap on an irregular erosion surface of Precambric rock; from 60 feet to more than 200 feet Se@etar then as can be told from the surface exposures the thickness of the beds between the Potsdam and the Mohawkian is from 300 to 350 feet. The most complete and continuous section of the upper beds of the Little Falls dolomite seen is that along the roadside east of Highland Park. Here the following section was measured. 108 NEW YORK STATE MUSEUM SECTION EAST OF HIGHLAND PARK 14 Gray, subcrystalline dolomite, with a small amount of calcite cement; great masses of gray to black chert at. summit, and in smaller amount at lower horizons; fre- quent irregular spots and films of coarsely crystalline calcite; to top-of ExpOSune.. sisnctae ee oy) tae 13 Medium coarsely crystalline, light gray ieloiite con- taining locally much gray and black chert; somewhat brecciated along ancient dislocation surfaces, the inter- spaces now filled by blackish, subcrystalline calcite... 12 Laminated layer of light and dark gray, subcrystalline dolomite, with small nodules of crystalline calcite. 11 Gray white, subcrystalline, hard dolomite, with freumient drusy cavities lined with dolomite, calcite and quartz crystals, quite like those in the Little Falls region, the dolomite crystals having formed first and the quartz last: oc 341i Woeuchelaoneyels oo OA muon ee ohare itera er The above section is shown in the Maple ave. quarry near Feet the fault line, at the north edge of Saratoga Springs; from the quarry the basal layer can be directly traced around to the north along the hillside to where it comes out on Broadway and forms the upper bed of the section shown down the hill toward St Clements. 10 Medium coarsely crystalline, gray to gray white dolo- mite, somewhat mottled in appearance, with some cal- cite cement between the dolomite rhombs; very full of CHEE chet a was bee See ee eke oe ee g Very massive, gray, granular to subcrystalline dolomite, full of large and small nodules of crystalline calcite... S Umexposedise One cai eta eluate 7 Massive layer of gray, granular dolomite with calcite spots, quitedlike that above gap.< 5... .....er 6 Dark gray, hard, finely crystalline Aiglenettes. bad smelt when freshly broken; occasional small cherts, and spots of crystalline calcite; very massive and irregularly bedded ..o °F 53 Ue sare lee epee tec co hee cae 5 Somewhat lighter colored than that above, less odor and with no chert, otherwise sumilamo8-0-\..... 0... oem Feet IO SIXTH REPORT OF THE DIRECTOR 1909 109 4 More of the dark gray, evil smelling dolomite, like that oe above; all is somewhat porous, the voids between the dolomite rhombs not thoroughly cemented up; there is pumas a Stall percentage of calcite cement.......... II IE Se eee is bk ev bet eee awe II 2 Gray, finely crystalline dolomite, lighter colored than that above and below, very massive, marked with dark col- meeeermtcs, aid Containino some chert...............% 15 1 Dark, blue gray, porous dolomite, at base of section..... I 11g This section terminates at the north in the angle between two branches of a fault, making it impossible to determine what thickness of similar beds may lie beneath. The light gray, crys- talline dolomites of the upper portion of the section continue on to the south through Saratoga, with likely some additional beds which do not appear in the section, but the thickness of such can not be great — probably less than 15 feet. Four miles west of Saratoga a hill composed of these same beds is capped by a cove limestone layer which is a great Cryptozoon reef, and which is likely at a somewhat higher horizon than any bed of the sec- tion; but it lies upon light gray, crystalline dolomites precisely like those which form the upper beds of the Highland Park section and can not be greatly higher than these. The best section of the lower beds, Potsdam sandstone and Hoyt limestone, is found along the Adirondack Railroad to the west of Saratoga. It is as follows, the beds being numbered from below upward: CONSECUTIVE SERIES OF SECTIONS EXPOSED IN CUTS ALONG THE ADI- RONDACK RAILROAD AND NEARBY QUARRIES BETWEEN GREENFIELD STATION AND SARATOGA 40 Exposures at Hoyt quarry; hard, blue to blue black, sub- crystalline to crystalline magnesian limestones, largely of dolomite rhombs with calcareous cement; I foot irom the top is a Cryptozoon reef, and the base is composed of another, the one shown by the roadside near the farmhouse, from which Hall originally de- meee fy ptozoon proliferum ; the rock is partly thin, and partly thick bedded; some of the layers IIo NEW, YORK STATE MUSEUM show coarsely crystalline calcite cement, giving large, a glittering cleavage faces on freshly broken surfaces; trilobites, Lingulepis and gastropods are found from bottom, tO Opi. cn 3 etal cee te tees Siena wees gener 25 One third mile north of the Hloyt quarry 1s anotnem ama face by the roadside, capped by the same Cryptozoon layer which forms the base of the Eloy quarry Section, : d Feet Inches 39 Dark blue, subcrystalline, magnesian limestone, full of Cryptozoon ; frequent, black oolitic grains. 1 5 328 Massive beds of blue, finely crystalline magnesian limestone, with occasional sand grains; trilobite TYASMICNES 2... bue wate aie ee oe 5 5 37 Thin bed of calcareous sandstone, weathering to brown TOCKeH \SIOME. «sacar ae ee SY cogs 5 36 Two beds of dark blue, crystalline, magnesian limestone with occasional sand grains.......... Zi 5 25, Layer ot datl ofay calcareous sanGstone. . ame aie I yi 34, Layer of light colored; vitreous sandstome wih films of darker material with calcareous cement jam 323 Dark colored sandstone with calcareous cement... 4 Ww [2 TO Four tenths of a mile northeast of this are two considerable cuts along the Adirondack Railroad in which the following sec- tion is shown. The hiatus between the two is estimated at 20 feet. Feet Inches 32 Dark blue, subcrystalline magnesian limestone.... 1 3 eq. Blackishrooliticidolomite£ on. eh). 7 - a tie cree eee i 8 20 Dark! blue, crystalline. dolomuter swarm. calleie cement, showing large, lustrous cleavage faces; hold si liei-meomaslse pits mec ciiltil tac tea: tee eae = lo 29 Black, oolitic Aisle mite: containing pebbles of mud linties totale: acinc oie eye he pean ee ER ee ee 8. 28 Rotten, crystalline dolomite, calcite cement rap- idby deachtiae. sO Wie cee ee ie 5 27 Blackish, oolitic dolomite in three beds the upper a Cryptozoon bed; frequent sand grains and many drusy cavities containing quartz and cal- cite ‘ery stalls >, SeheOe Soees ew ere 2 6 SIXTH REPORT OF THE DIRECTOR IQOQ IIl : j } Feet Inches 26 Easily rotting, crystalline dolomite, calcite cement, (21211 5 iO Sar a 9 meieatd, light colored, vitreous sandstone.......... I 4 24 Crystalline, bluish dolomite, poorly cemented by RR EME eis eins Sey bs oe cee Ce se eee I 7 23 Two massive beds of blackish, subcrystalline, magnesian limestone, with frequent sand grains, UCM ESTCTV"CULdn 62 faeces ele wlee ae oh eae 4 3 22 Concealed between the two cuts; boundary be- tween Hoyt limestone and the passage beds to the ee SOCIO a5. eee sb ec ele oils weve we wie fe 20 21 Rotten, brown, calcareous sandstone, blue when CORE. SS ee ee ae eee re ee 8 20 Hard, vitreous, light colored sandstone, banded with narrow streaks of darker colored sandstone Meee IGAneCOUS CeIleNt, .3 6.02.0 6s eee 2 4 19 Thin bedded, blue, calcareous sandstone, weather- Re UTS ID ow. ee ieee dle se hy beads ee oe 9 febine black, oolitic dolomite, frequent rounded tiieGcercrains, many small drusy cavities....... I B 17 Blue, calcareous sandstone, weathering hght col- aanoper portion shaly.......b0h...6..006%. I 8 Seeieatda, eht colored, vitreous sandstone.......... eit 6 15 Thin bedded, calcareous sandstone, somewhat oolitic, blue when fresh but rapidly weathering brown-mottled and crumbly, many drusy cav- ities, with calcite and quartz crystals; abundant trilobite fragments, constituting the lowest zone of these so far discovered near Saratoga......... i 3 Sueeiecoloted, vitreous sandstone............... 2 5 13 Bluish, nodular, finely crystalline dolomite, with a Slight amount of calcite cement, shaly at top and bottom, with frequent nodules of crystalline Steweeeniolds Lingulepis acuminata. 2 6 Meeeremt colored, vitreous sandstone............... 3 It Gray, banded sandstone, slightly calcareous...... 3 9 10 Alternating calcareous sandstone and crystalline dolomite, of blue gray color, large nodules of Beyeraiiine calcite in the latter; base of cut.... 3 9 Concealed between this and the next cut to the SO) ITZ NEW YORK STATE MUSEUM ? ; } Feet Inches 8 Hard, vitreous, light colored sandstone, with darker calcareous sandstone above and below.. 1 8 Concealed to brook exposures next east; arbitrary boundary between passage beds and Potsdam in the interval \ta bores secre ee oer wine ee ee 30 N 6 Light colored, vitreous sandstone, with alternating layers of darker, calcareous sandstone which weather rapidly. sh.) ae a te ape ee 30 5 Light colored, vitreous samdstonesd) sane 5 aConcealed (iac.cck eee ae ee ae oa anes 4 2 Light colored, vitreouscsamdstone: 2... Seer. B 2 Concealed’s fe a ee ee eee 4 I Conglomerate, increasing in coarseness downward, and reaching nearly to the base of the formation. 10 In this section we find then a thickness of 94 feet, 1 inch of the Hoyt limestone member of the Little Falls formation, counting in with it the 20 foot gap between it and the passage beds, with the summit of the member not reached; beneath it a thickness of 52 feet, 1 inch of what we class as passage beds, counting in with them the 30 foot gap between them and the Potsdam; and finally 96 feet, 8 inches of Potsdam with the base not reached, though it is unlikely that as much as Io feet lies beneath. We find es- sentially the same trilobite fauna ranging through a thickness of at least 100 feet, commencing in the passage beds and continuing up through the entire thickness of the Hoyt limestone. There is a ~ measured thickness of 119 feet of Little Falls dolomite above the Hoyt member in the Highland Park section which shows neither the base nor the summit. We are, however, disposed to think that the entire thickness of this part of the formation is not greatly in excess of this, and that the coarsely crystalline, light colored dolomite of the upper part of the Highland Park section consti- tutes the summit of the formation about Saratoga. In the north- ern part of the village just south of the quarry which furnished the top of our measured section and close to the fault are a few thin patches of Mohawkian limestone, resting upon these upper beds and apparently directly deposited upon them. The Mohawkian is a conglomerate with many pebbles of the underlying dolomite. The horizon of this contact is certainly not more than 20 feet above the top of the quarry section. SIXTH REPORT OF THE DIRECTOR IQOQ 113 The thickness of the beds that may lie beneath the bottom of the Highland Park section and the top of the Hoyt limestone mem- ber in the Hoyt quarry, in other words the thickness of the beds belonging between the base of the former section and the top of the latter, is much less certain, but so far as can be judged from sections elsewhere the amount is not great. Estimating the Hoyt at a maximum of Ioo feet and the upper member at about 150 feet, the total thickness of the Little Falls formation in the vicinity of Saratoga may be set down as approximately 250 feet. The maxi- mum may fall a trifle under this figure, but it is quite certain that it does not exceed 300 feet. Locally, however, on account of Pre- mohawkian erosion the thickness may be considerably less. At Rock City Falls, 7 miles west of Saratoga, contact with the Mohawkian is well exposed. Here this Ordovicic limestone rests upon darker colored dolomites of the Little Falls formation which - seem to belong beneath the coarse, whitish rocks of the upper por- tion. Midway between Saratoga and Rock City Falls are other exposures which show Mohawkian limestone resting on similar beds, though the higher, coarse grained, whitish beds are near at hand, and in such situation that we can only interpret the exposures as indicating that the Mohawkian was deposited on an eroded sur- face of the Little Falls dolomite, beds being absent in some sec- tions both above and beneath the unconformable line of contact tat are present in others. The evidence seems clear to us that the whitish summit beds of the Little Falls have been eroded away locally, the Mohawkian in such cases resting on lower beds. The lower part of the Mohawkian varies greatly within and in areas adjacent to the Saratoga quadrangle. As a rule the basal Mohawkian beds in this region have been assigned to the Trenton, Dut, so far as observed, they are in all cases older than the low- est Trenton in the type sections on West Canada creek. At the same time, however, the first Ordovicic bed to follow the Little Falls dolomite, or the Tribes Hill formation and the thin irregular wedge of Lowville where these are present, is younger than the Watertown limestone (“7 foot tier”) of the Black River group. In other words, in the area between Saratoga on the east and say Canajoharie on the west, the post-Lowville Mohawkian begins with beds that are wanting along West Canada creek and Black river. At Saratoga a 6-10 foot, heavy bedded crystalline limestone is found either resting on or not more than 5 feet above the top of the Little Falls dolomite. At Rock City Falls, 6 miles west, this bed Ii4 NEW YORK STATE MUSEUM lies about 30 feet above the dolomite, the basal layers of the under- lying interval being unquestionably of the Black River group but not so low as the Lowville and probably also younger than the Watertown limestone. The Lowville is represented by 2-4 feet of beds at Tribes Hill in the Mohawk valley, but here the crystalline limestone is only 3, to 5 feet above it. The section at this locality differs further in that it contains an unusual thickness (13 to 18 feet instead of 2 to 10 feet) of somewhat shaly limestone above the crystalline bed before the Prasopora simulatrix fauna, with which the typical Trenton begins in New York, sets in. This irregularly distributed, presumably late Black River formation, in-~ tervening between the true Trenton above and the more typical Black River formations (Lowville and Watertown) beneath, will be fully described in another paper. Here it will suffice to say that it wedges out westwardly in the Mohawk valley before reaching Little Falls. So far as known its maximum aggregate thickness is about 60 feet, the lower 46 feet of which is exposed at Rock City Falls. A good thickness is shown also in the section at Glens Falls. The work of Prof. W. J. Miller on the Broadalbin quadrangle (next west of the Saratoga quadrangle) in 1909 shows that there the Hoyt limestone is absent from the section, being replaced by unfossiliferous dolomites and probably also by beds included in an increased thickness of passage beds between the dolomite and the Potsdam. The well drilled at the Hathorn spring in Saratoga a few years ago is reported to have begun in the Trenton limestone and to have passed through some 700 feet of limestone before reaching the Potsdam. This is a thickness at least 300 feet greater than the surface exposures indicate. The well is near a fault and it seems probab!’e that it crosses a branch of the fault in such wise as to re~ peat a considerable thickness of the limestone. Section at Whitehall Whitehall is between Saratoga and Ticonderoga and thus, from the standpoint of distance, serves as a convenient intermediate point between the two. The district is much faulted, but a good, con- tinuous section is afforded from the Precambric up through the Potsdam and well toward the summit of the Little Falls dolomite, simply by ascending the hill known as Skene mountain, a fault block whose summit rises sharply to more than 400 feet above the level of Wood creek. Walcott has given a detailed section of the Pots- Si REPORT OF THE DIRECTOR I9Q09 I15 dam and passage beds at this point and a more generalized section of the dolomites above.t We were more concerned with the upper part of the section than with the Potsdam and made the following measurements down the south face of the hill, where the section seemed most complete: Peon OF LITTLE FALLS DOLOMITE AT. SKENE MOUNTAIN NEAR Nein RATE. IN ny. Feet 7 Whitish, rather coarsely crystalline dolomite, with a little chert at summit; this material forms the summit of the knob everywhere and is of greater thickness than ro feet, that being only what is shown where the section was meas- Sry i aiels te a em Peels Were baw eh 10 6 Mostly very finely crystalline, dark gray magnesian limestone somewhat cherty above; full of irregular seams of more coarsely crystalline material which weathers less readily and forms projecting films on weathered surfaces; lower portion very massive forming high cliff; at base a single Peememenaeiment was fOUNd ke QO 5 Very coarsely crystalline, whitish dolomite, somewhat oolitic and becoming steadily finer grained downward.......... 20 4 Gray blue, finely crystalline dolomite with calcareous cement, weathering sandy looking, many calcite-filled cavities; at EEE Min PLOZOGN WOLIZOM. 6 2 5b ke es hee es oe 50 Pines @olitic,magnesian limestone.......0.....06..005- 20 REMPETMIGMACCAICH fe. cic deine adhe dee gc cee eek ee eee 50 I Passage beds: chiefly- calcareous sandstone, but with alter- nating beds of vitreous sandstone and blackish, crystalline, sandy limestone; only a 15 foct thickness of these shows on the south face but, followed around to the west side the full thickness comes in with the large thickness of Pots- dam underneath which Walcott measured, the dip being strong to the east This section is much like those at Saratoga and Ticonderoga. The horizon of the Hoyt limestone is largely concealed, but the black, oolitic beds above the gap are exceedingly like those as- i mys. Geol. Sur. Bul. 81, p. 345. 116 NEW YORK STATE MUSEUM sociated with the Hoyt. Beds 17 to 24 of the Ticonderoga section are thought to represent the same horizon. Walcott reports Lin- gulepsis acuminata in the passage beds. All the upper portion of the section has the typical characters of the middle and upper parts of the Little Falls dolomite, but unfortunately the summit is not quite reached. Loose chert, apparently from the upper part of the dolomite, found 2 miles northeast of Whitehall, contains two gastropods and a cephalopod that mark the middle part of the Ozarkic in Missouri. The same beds there contain trilo- bites closely allied to those found in the Hoyt limestone near Saratoga. In the National Museum is a small collection of fossils made by Walcott from 2 miles north-northeast of Whitehall which contains a half dozen specimens of the fauna of division D and demonstrates the presence of at least that member of the Beekmantown. Since Whitehall is due south of Ticonderoga and much nearer that point than Saratoga, it is quite likely that other members of the Beek- mantown were deposited in this region. F Mohawk valley sections Passing southward from Saratoga to the valley exposures the Potsdam sandstone rapidly thins and disappears, letting the passage beds and then the Little Falls dolomite down on the Precambric. The manner of disappearance seems to us to in- dicate plainly that the Potsdam vanishes because of overlap, and that the dolomite of the valley is the direct equivalent of that of the Saratoga and Ticonderoga sections and wholly above the Potsdam. The paleontological evidence, so far as it goes, con- firms this belief. , In the most easterly of the Mohawk valley sections a lime- stone formation of considerable thickness, the “ fucoidal layers ” of Vanuxem, overlies the dolomite. This limestone is thickest at the east and thins westward to complete disappearance west of Little Falls. The published sections of Prosser and of €le- land, with the faunal studies of the latter, leit no doubt of the fact of the general persistence and equivalence of both the dolo- mite and limestone formations throughout the valley, hence our ' comparative study seemed to call for sections only at the east and west ends respectively. We measured and studied sections at Tribes Hill and Cranesville at the east, and at Little Falls, Middleville and Newport at the west. SIXTH REPORT OF THE DIRECTOR IGOQ SHETICN AT CRANESVILLE 19 Irregular, thin bedded, crystalline limestone, with Solenopora compacta and other fos- RI OL wel able dc ei eek visi a8 o's 18 Thin bedded, fine grained, somewhat argillaceous limestone often nodular; contains Tetraditum; 4 17 More coarsely crystalline, otherwise like that just Go iar each Pte tube ns ee wee oo ole 16 Massive, blue gray, subcrystalline limestone, often lumpy, with abundant, subangular lhmestone pebbles from the dolomite below; many fossils, Maina Letradiim etc.; 6 to........ 00.005 15 Dove limestone of Lowville character, often not memeeeme base of Lowville; 0 to............. Unconformity 14 Thin bedded, earthy, gray dolomite, weathering oe SRS oe It ee eee bale es 12 Sandy, laminar, gray dolomite, containing O phi- PeepmMe Me (TC Ha ee E itorah eg: Ee ba ee eh ee ee es @emadra, Die stay, fine grained dolomite........... =o 8s PRS Ss Selaminar, fine grained dove limestone, mottled with strings and patches of argillaceous dolo- mite, suggesting fucoids; contains Eccyliom- se lea ora ER SS a a 6 Thin bedded, alternating limestone and shaly lime- stone, with pure limestone at base; many fos- Sils, chiefly gastropods; base of Tribes Hill..... Unconformity 5 Whitish, rather coarsely crystalline dolomite on illside between the forks of the road............ ates ee eh ok sic aks cae weleicc ows. 3 Thin bedded, argillaceous, gray dolomite, very irregular above and with rolls in the lower por- tion eae eee ES Ye See eee. 6 6 00 8 e)y6, Of oe « a 8 elle! la Feet IO EL7 Inches 118 NEW YORK STATE MUSEUM : ; Feet Inches 2 Light to dark gray, crystalline dolomite, many nodules of crystalline calcite, often large; many of the beds have calcareous cement and weather porous, crumbly and sandy looking: ~-:— 7a 20 1 ConcealedttosievelsoliWotianiicyi. tc Go wees go Though this section is very imperfect, yet. it gives both the upper and lower contacts of the Tribes Hull limestone witha thickness of 168 feet for the formation in this section. The base is well shown and is distinctly unconformable on the dolo- mite beneath. The Little Falls dolomite has the general char- acters that it shows in all sections, the coarsely crystalline, whit- ish beds above, and darker, finer grained beds below. The base of the dolomite is below the river level, but it is quite certain that the Potsdam is still im place beneath, ~ (ine) Witeperdemas sheet, midway of which this section occurs, corners on the Sara- toga sheet at the southwest and is distant only 20 miles from the Saratoga section. On the Broadalbin sheet (north of Am- sterdam and west of Saratoga) Miller finds the Potsdam run- ning all the way across the sheet from east to west. The section differs from that at Saratoga chiefly in that the Dribes eam formation has come in between the Little Falls and the over- lying Mohawkian. It differs from the Ticonderoga section in that none of the Beekmantown except the Tribes Hill division appears. The section was measured up the creek which comes into the Mohawk at Cranesville from the north, diverging from the creek up the left-hand road, 1 mile north of thegmyes Cumings had previously published the same section though we subdivide somewhat differently and find the thickness of the upper part less than he gives it.t Section at Tribes Hill At Tribes Hill, 8 miles west of Cranesville, we also measured the section. ‘The locality is just across the river from Fort Hunter, where the original discovery of the fauna which Cle- land described was made.? The section at Tribes Hill is much less complete than at Cranesville, but we have chosen it as the type locality because of the excellent exposure of the character- istic fossiliferous limestone of the formation which is found UN: Y. -State: Mus, Bull 245 .peaa Am. PalkoBilen gen mo sense SS ee eEeeEeEee—E EE SIXTH REPORT OF THE DIRECTOR 1909 I1g along the creek which flows southeast through the village. This section was carefully measured by Cleland and as here given is practically a reproduction of his, a few lithologic data being added.* Pee iioN IN CREEK NORTH CF METHODIST CHURCH, TRIBES HILL ; : Feet Inches 7 ayer oi compact, dove limestone, probably Low- Ss a 2 so ee SS 4 Unconformity Seeather dark gray, hard, fine grained, somewhat laminar dolomite, breaking with conchoidal frac- Sw Eye a 2 8 Alternating dove limestone and sandy, laminated, magnesian limestone, in undulating, irregular layers; main horizon of Dalmanella wem- Me cae ies nee en bee 7 ii 4 Argillaceous, yellowish dolomite, or magnesian limestone, capped by a 1 inch layer of limestone Memrmonmenaiier With) LOSSIIS, 2... ek ee ee ee 4 Winely granular, blue limestone, which is conglom- O1 €3 eratic and oolitic, and exceedingly fossiliferous ; apumdant Ribeiria and small gastropods........ 2 6 2 Massive, slightly argillaceous, gray, magnesian lime- emer men occasional Lossils. 2. ce a le 7 5 1 Blue gray limestone which 1s somewhat conglomer- atic and contains fossiis in considerable number... 3 I This section furnishes a thickness of 37 feet, 3 inches of these mepmeat tossiliferous beds. The base of the section is nearly 200 feet above the river level, but the underlying beds are ex- MoOsed in very fragmentary fashion. The dip is strong to the west and brings this horizon down to the level of the railroad at the Tribes Hill depot. A short distance east of the depot is a considerable quarry in these beds which was carefully meas- ured by Prosser. There are also quarries just west of the depot where the Lowville and overlying limestones are well shown, with the summit of the Tribes Hill limestone beneath. In both tliese sections there is a thickness of from 15 feet to 20 feet of gray, magnesian limestone and dolomite at the summit of Zee eal Bul. v. 4, no. 18, p. 6-8. “N. Y. State Geol. 15th An. Rep’t, p. 645. I20 NEW YORK STATE MUSEUM the Tribes Hill which certainly differ from bed 6 at the top of the formation in the section in the village just given. As the Lowville and other Black River limestones are thicker in the quarry at the depot than in the village section it is thought likely that, in part, the westward dip may signify descent of the beds into an original synclinal basin in which the Tribes Hill formation retained beds that were eroded in nearby areas. Western sections It was our intention to study the section at Sprakers about mid- way of the valley, where the Precambric is brought up on the west side of the fault, and the full thickness of the “Calemencies gas shown. We were, however, unable to do so and hence can not state whether the contact between the Little Falls dolomite and Tribes Hill limestone is here exposed or not. However, consider- ing that wherever observed the formations maintain unconform- able relations to each other there seems no reason to doubt that similar conditions will be found to obtain also at Sprakers. Prosser has given two carefully measured sections at this point, one of the cliff at the West Shore Railroad cut, the other along Flat creek.? The Potsdam is absent, having disappeared through overlap. The first section shows a thickness of 490 feet, the lower 385 feet of which belong apparently to the Little Falls, the upper 40 feet be- long certainly to the Tribes Hill, while between the two is an in- terval of 65 feet with infrequent exposures which in all probability belongs mostly or entirely with the Tribes Hill. The summit of the formation is not reached. Prosser reports Cryptozoon about 200 feet above the base in the Little Falls, and the Tribes Hill fauna in the upper 4o feet of the section. The Flat creek section, capped by Mohawkian limestone, shows 190 feet of rock, the upper 95 feet ci which Prosser assigns to the Tribes Hill (fucoidal beds) and the lower portion to the Little Falls. Except for lack of knowl- edge in regard to evidence of unconformity between the two forma- tions and the precise horizon of the break, the section is perfectly clear. ; Section at Little Falis The best section at Little Falls is that along the creek to the northwest of the town, where the upper beds and all the contracts 1N. Y. State Geol. 15th Ans Rep’t, p. 641-43. SIXTH REPORT OF THE DIRECTOR IQOQ 121 ate fully shown. The contact of the Little Falls dolomite on the Precambric is also shown, but a complete section of the dolomite The creek is nowhere to be found on the north side of the river. section follows, commencing at the base of the Trenton. SECTION IN SMALL CREEK AT NORTHWEST EDGE OF LITTLE FALLS mee or Prasopora simulatrix bed of Trenton Hiatus 20 Brittle dove limestone; normal Lowville........... 19 Basal, less typical Lowville beds; dove limestone with many rounded quartz grains, in increasing amount TW SP BLIPCL gee ener Sane a Ss ao ial © wl Gl eae oS a 8 Hiatus 17 Thin bedded and somewhat shaly layers of dove lime- stone and dove limestone conglomerate, the pebbles of which are embedded in crystalline limestone; considerable pyrite; found two trilobite fragments. 16 Thin bedded, hard, brittle, blue dove limestone with shaly partings; full of stems and plates of cystids and with fewer gastropods (Ophileta le- vata ) and trilobite fragments in very bad preser- LTS). 22 SSI eee ee aaa 15 Iwo massive beds of bluish, finely granular lime- stone, somewhat mottled with crystalline seams; rude fucoidal markings on surface; contains fPerenoromaria hiunterensis......... 14 Similar to above, somewhat less like dove limestone, fine wormlike tracks on surface, upper bed weather- Seeder but unevenly laminar............... 13 Massive, 1 foot to 2 foot beds of dark, blackish gray, firm, hard, fine to medium crystalline dolomite, eerie black “streaks... os ke ee 12 Finely granular, gray dolomite, some beds having cal- careous cement and weathering reddish and sandy looking ; it is unconformable with the irregular sur- faced layer beneath, whose surface the stream fol- lows for some yards, the slope being greater than the dip of the beds above, so that an additional 6 foot thickness comes in; where thickest the basal Feet Inches 1et 1G 122 NEW YORK STATE, MUSEUM om IK@) N layer is a conglomerate, with large but thin black pebbles in a reddish, calcareous matrix; in the lower portion of the bed the pebbles lie flat, but above they are disturbed and may stand on edge; base obal ribessidni 2A eeitio. pec eee Hard, finely granular, gray dolomite, with coarsely Leia Dy OST ACE OF BOs. eet area oe ne ee Hard, finely granular, massive, gray dolomite, with some calcareous cement, and weathering reddish; a strone chert ped at te summit. ae eee A ponderous Cryptozoon reef of varying thickness, heavily silicified forming variegated black and gray chert; its upper irregular surface is thinly covered with gray, crystalline dolomite; beneath is a vary- ing thickness of from 4 to 7 feet of finely crystal- line, darlvieray dolomite: so. aa Porous, blocky, gray dolomite, dolomite crystals in calcareous cement, weathering whitish; many sand OCAMMS AL Ate ol ce ae pana CO ier en Gray, finely crystalline, porous dolomite, calcareous cement; drusy cavities with dolomite, calcite and Quartz “crystals -— iredtlent dtlartzsonatls: sont stale upper and lower surfaces of the beds; holds thin, twisted chert plates which suggest Cryptozoon.... © Binely crystalline. ray cdelonmitea paren re Medium coarse grained gray dolomite, weathering sandy looking because of calcareous cement; a Crypitozoon weer. al) DASE cess. 4 o -encca ee eee ee Comcealedins is ise cee Baia, OCU eis ee atte Medium coarsely crystalline, gray dolomite with cal- careous cement; thin chert seams of Cryptozoon character ain’ ie uppemeportiOn.r . cls. Senet Coneéaled? 2 araie separa yoo. oa. loos oe Light gray, rather coarsely crystalline dolomite, with some ‘rounded grains of quartz sand, in 6 to 1S inch: layers; Veement 1m panemcaleancons , —aievmne streak of very black, shaly material near base; fre- quent, “blackish. diriisy cayanlesmem sera. oan ree ‘Feet 30 24 IO 1G) NW 30 Inches This section does not reach the base of the formation, but th lower beds are well shown in the eastern portion of the town with SESii REPORT OF THE DIRECTOR I9Q09 123 an additional thickness of some 150 feet. Almost at the base is the shaly zone with Lingulepis acuminata, first reported by Shaler and H. S. Williams. ‘Though the outcrops are not entirely satisfactory, there is reason to believe that the unconformity at the base of the Tribes Hill limestone locally descends in this vicinity to the top of the ponderous Cryptozoon chert included in bed 9 of the above section. This condition is suggested on the ridge just west of the creek. That the floor on which the Tribes Hill was laid down was uneven is shown by comparison of the two detailed sections made on the north side of the river in the bluffs back of Little Falls. In the section exposed in the creek on the northwest edge of the town, as above described, the Tribes Hill has a thickness of about 50 feet. The silicified Cryptozoon reef of the Little Falls dolomite, which seems to be a persistently marked zone in this vicinity, lies here about Bo feet lower, hence 80 feet beneath the base of the Lowville. Hess than 200 feet to the west the 30 foot interval is reduced to about 18 feet. The basal bed of the Tribes Hill (no. 12 of section) memes reduced trom 30 feet to about 16 feet. In a branch of this creek about 1/6 mile east, the Cryptozoon bed is only 58 feet beneath the Lowville and only 21 feet beneath the base of the Tribes Hill, which, therefore, is but 37 feet thick at this point. The Mjeeeor 12 feet, when compared with the section in the main branch of the creek, is found to be divided between the top and bottom, beds 16 and 17 of that section, aggregating 5 feet, being absent here. The other 8 feet probably are lost from the base, though the character of the middle and lower beds of the Tribes Hill varies rapidly from place to place so that the individual beds are not easily recognizable. A mile farther east, along the road to the quarries northeast of Little Falls, the Tribes Hill seems even thinner, but the exposures are too poor and the dip not sufficiently regular to permit a definite statement on this point. In mapping the Little Falls sheet it was shown that the dolomite formation rapidly thinned because of overlap, in passing across the quadrangle from south to north. It was at that time supposed to be a single formation, and the loss by overlap was supposed to be at the base. Since, however, we are dealing with two, uncon- formable formations it may well be that both thin northward be- cause of overlap, and that the Tribes Hill disappears before the Little Falls does, letting the Lowville down upon the latter. Until the quadrangle is restudied it is impossible to definitely pronounce 124. NEW YORK STATE MUSEUM upon the matter. A study of the section at Middleville, 9 miles northwest of Little Falls, seems, however, to indicate that both formations thin to the north owing to overlap, and that the Tribes Hill pinches out long before the Little Falls does. In the Middle- ville section the Tribes Hill has apparently disappeared; certainly the fossiliferous, dove limestone beds do not occur. Since the formation still has a thickness of 50 feet at Little Falls and has not been thinning westward from Cranesville at a rate exceeding 2 feet per mile, it is not impossible that this sudden disappearance is attributable to the distance north, rather than the distance west from Little Falls. However, in mentioning the average westerly reduction of the formation it is not to be understood that we regard this as taking place gradually. On the contrary, as intimated in the preceding paragraph, the warping of the underlying surface of Little Falls dolomite renders the suggestion of gradual diminution quite impossible; and the same reason might very well cause rapid thinning west of Little Falis. At Middleville we measured the following section up the creek which comes into the town from the east: SECTION AT MIDDLEVILLE Feet Inches 25 Trenton limestone with Dalmanella common in lower 6 feet and “Ptasopo ra sim ula tedes abundatit. above’ (hates. eee en eee 60 Hiatus | 24 Thin bedded, dove limestone with irregular summit ; abundant Phytopsis, and Tetradium cellu- Losi) typical dcowville: 2. ee 13 2a OW ONCCAEd Vike Saw ta een on ate wee ee 2 22 Thin bedded, light colored, sandy limestone with abundant quartz grains; much bored by worms of large size; upper 2 inch layer a calcareous sand- stone, at base of which worm tubes cease; 1 foot, GTN Che s tite pene ees aet ts Sloss ass ees eee 2- 2 21 Cobbly, conglomeratic, calcareous sandstone, black to brown’ tn col@t ttre pate: ee acts + ae 10. 20 Irregular bed of calcareous, small-pebbled quartz conglomerate ; base of Lowville................. I Hiatus and unconformity 19 Compact, very fine grained, light bluish gray dolo- 14056 5 RRR EMER En on 6 theres Nh Fu eas aN al 3 SIXTH REPORT OF THE DIRECTOR IQOQ 18 Alternating beds of light gray, finely crystalline dolo- mite and of more sandy, darker colored material; midway is a heavy chert bed, with both black and TE eo Sis ek ies ee ee oe we 17 An irregular bed of light gray, finely crystalline dolomite, laminated and weathering to finely lined surface, filling irregularities in surface of preceding RTM 22S Sala gee Vela ee we Sn 16 Very nodular and irregular bed of gray dolomite, | with many sand grains and with cherty looking Metres Or black, silicified sand; 5 feet‘to......... 15 Chiefly very light gray, calcareous, sand rock, but 1 with alternating seams of darker colored dolomite. 14 Light bluish gray, finely crystalline, drusy dolomite ; : very PeMAMS eck es Mee ee ee 13 Very dense, fine grained, light colored, very sandy dolomite, full of rounded grains of quartz sand; RememGURGSN CAVITIES. 0S ee te ee ee ‘12 Porous, very light gray, finely crystalline dolomite, with many sand grains, and frequent green specks ; many drusy cavities with quartz crystals in upper RE ees ate ees b euv't Sab cre nye bb wy oe Ii Massive, gray dolomite, with many sand grains.... ‘Io Very fine grained, mottled, light gray dolomite.... 9 Dark gray, very quartzose, massive dolomite........ 8 Massive, somewhat porous, dark gray dolomite; sand grains fewer than in the beds beneath, but larger iene ee kg eg ea eee 7 Light gray, thin bedded, very sandy dolomite, with black streaks running through it; full of sand grains; one thin, hard, fine grained layer 4 feet 8 ES eee nee ni ae EE EQUI l o ild e we ec ve ee Cenc wee 5 Rather massive, porous, blue gray, crystalline dolo- mite; frequent crystalline nodules filled chiefly EEE Noe oe ae ds eed she see ews ss 4 Massive, Cryptozoon reef layer; blue gray, porous memcnaite with nodules of calcite.:...........04. Mee Stay, porous, crystalline dolomite............ MMOL ns ccc cs Oe ec ene es Feet io) IO CON UI Ww I2 60 me tn 25 725 Inches 1) On IO 126 NEW “YORK STATE MUSEUM.- : Feet Inches | I Massive, finely crystalline to granular, gray dolomite, | with large-calemte modileset. ts .9 a ere eee 3 Interval to surface of Precambric in West Canada creeks about Prk ton Bch inn see meee ae eer 50 In this section, including the concealed interval at the base, we have a thickness of 231 feet of Little Falls dolomite, as measured from the base of the Lowville down to the level of West Canada @ creek, which is substantially the base of the formation. There is nothing that we could definitely correlate with the Tribes Hull 4 limestone as already stated. The thickness here is just about half — the combined thickness of the two formations at Little Falls. 7 Since at least 50 feet have gone from the summit it seems to us clear that the thinning in this direction 1s not due simply to over- lap, but represents a loss both above and beneath; that is that each of the two formations thins northward, and that the Tribes Hill has thinned to the vanishing point. It will also be noted that there is here a thickness of nearly@ 19 feet of Lowville and that the Lowville is directly followed by | the Plectambonites and Prasopora bed of the Trenton with no sign of the older beds, which in the Mohawk valley have usually — been referred partly to the Black River and partly to the Trenton Four miles northwest of Middleville along West Canada creek is Newport, and here the most—westerly of the good sections, exposing the horizon with which we are especially concerned, is — found. The exposures are in the creek bed, the railroad cut justi south of the depot and in Dunn’s quarry a few rods west of the depot. SECTION AT NEWPORT Feet — Inches 12 Crystalline, highly fossiliferous, gray limestone bands alternating with black argillaceous nodular lime- stone and a little shale, Plectambonites very abund- ant basal) (irentone cs. 0 ss ee eee 2 6 Hiatus | 11 Blocky, nodular, fine grained limestone, black lime- stone containing Columnaria and Streptelasma ; has heretofore been referred to as “ Black River ” but represents the Leray limestone member of the Lowyille formation im jletrersom county ea: 54. Z a Small hiatus SIXTH REPORT OF THE DIRECTOR 1909 127 ee ; Feet Inches TO Brittle, cove limestone, of ordinary Lowville char- Meeemtioor Fiytopsis tubes. .............005.. 1 9 Brittle, dove limestone, with occasional sand grains in the basal layer; slightly impure as shown by irregular laminations on weathered surfaces; Memwariim cellulosum occurs below , LD. a6 cSt Sani a 6 ie meeconcealed except for the surface of one layer at base, which is slightly impure dove limestone, with Beare tC TAINS. 6. be ee ce os I 9 GL re Bl 6 Thin bedded, light colored sandy limestone and cal- careous sandstone; shaly partings; probable base LL Sues Sarena 4 6 Hiatus and unconformity eg 5 on cs ke go el vce ee te aes 20 4 Massive, gray, drusy dolomite; quartz sand grains.. 1 6 3 Irregular, massive to thin bedded, sandy, gray dolo- mite; many druses above; many sand grains; cer- tain layers mottled and laminated with black.... 13 RE TO oe ee ha eet es 15 I Massive, granular, blue gray dolomite, but few. sand eras, Cryptozoon and much chert in lower 5 I ee er Mas 8 Here we find the Lowville thickness to exceed 28 feet, as against fie 15 feet shown in the Middleville section; we have also beds intervening between the Lowville and the Trenton which do not appear in the Middleville section. But as in that we find no trace sor the Tribes Hill formation, the Lowville resting on the Little Falls dolomite. In these western sections of the Little Falls dolomite, we miss the light colored, coarsely crystalline beds which form the sum- mit of the formation at the east. Whether they were deposited and eroded before the deposition of the Tribes Hill, or whether they change laterally into finer grained, gray beds on passing west, We are not sure. Since the formation shows no diminution in thickness it is perhaps more probable that the latter is the case. Theresa formation This name was given by Cushing two years ago to the passagé beds and overlying magnesian limestones which occur between the 128 NEW YORK STATE MUSEUM Potsdam and the Pamelia formation (upper Stones River) in the Thousand Island region.t The formation as defined is thin, not over 60 feet, seemed a unit and was thought to be entirely older — than the Beekmantown. In its lower portion a variety of Lingu- lepis acuminata is abundant, while the higher beds contain - cystid plates and a large, flat gastropod. These now prove to be 4 identical with the cystid plates and the Pleurotomaria hun-~ terensis (Cleland) which are found in the Tribes Hill lime-~ stone of the Mohawk valley, whence it follows that the upper por- — tion of the Theresa formation in Jefferson county is of lower Beek- 5 mantown age. We are, however, of the opinion that the lower — portion is properly to be classed with the Potsdam beneath as of © Saratogan (Ozarkic) age and that there are two formations pres- ent instead of one. We also think that an unconformity will be — found between the two, now that it is suspected, so that search 9 can be made for it. It is, therefore, unfortunate that a name was given to the supposedly single formation. We suggest, however, © the retention of the name Theresa as a designation for the passage — beds which occur everywhere in New York between the Potsdam and the overlying Little Falls dolomite, since they have a char- acteristic lithology of their own, and should be and can be mapped ~ separately. . Correlation of the foregoing sections In order to bring out more clearly and concisely our ideas in re- gard to the sections, they are given in generalized form in the ac- companying table. The Little Falls dolomite occurs in all and in ¥ fairly uniform thickness except at the extreme west where it is” thinned by overlap on the Precambric. The Tribes Hill limestoney overlies it in most sections, but thins westward to disappearance in the Mohawk valley; the Saratoga region seems to have been just beyond the reach of its deposits. Correlating the Tribes Hill with the typical dove limestone of division B of the Champlain © Calciferous, then sedimentation would seem to have been only — locally interrupted in that trough as noted in the vicinity of Ticon- deroga. But, if the former is older than the latter, as 1s indicated : by faunal evidence, then the whole of the Champlain valley was emerged while the Tribes Hill was being deposited in the Mohawk valley. The Tribes Hill and Little Falls formations seem everywhere ~ unconformable in New York, and we make this unconformity the — “Geol, Soc’ Am. Bull aos Essa70. 129 auojspues Wepsjog UOTEULIOF esalsy y, i a}IULOTOp AAG ESM netd alk ee Gletr peyueseider Jo Juesqe CMG rear UMOJULUTII0G Sith REPORT OF THE DIRECTOR 1909 VOOUAGNOOIL Quo }SpuULS wIRps}og UOTLCULIO} esoloy L, Q}IULO[Op SHysal srt UMOUYUL) (He 02) G@ Ald UMOJULTIS II “Aqqe TIVHALIHM ‘OIGUIvIITG UO ATGVULIOZUOOUN $4sui UOTJOOS TORY | ee NIla@1Tvadvoadd Ci rie TTIH SHdlaL Saaavads STI1TVa ZILLI GHTIASANVAO suo12as {0 J4vYyD auojyspues auo spurs we ps}og wWeps}og UOT}CUIO; UOlJCULLOF esaloy L, eseloy ], ‘sounl] JAOPT a}IULOTOp a}IULOTOp 9}iULO[Op 9}ULOTOp SS ea See UTA SHEE Tal SHAE SIE QUOJSOUT] 9UOJSOUTT SUOJSOULT WTS Ueh WET Cian IE, UE Se. ULIO;UOOUN UOTPOS Yo sdvo 9UOJSOIIT ULIYMBYOT 1OYJO IO ‘AT[IAMO’T Joy 1D © ey rab) ct o { 0 ab) O}IMUOTOp eae Ea eae ee A}UTLOJUOSU Fy) e) i} on ° a g. @) aTTIAYTACIN LYOdMUN 130 NEW YORK STATE MUSEUM - dividing line between the New York representatives of the Sara- 9 togan (Ozarkic) and the Beekmantown (Canadian). In the Cham- plain region the higher divisions of the Beekmantown occur, but they are utterly lacking in the Mohawk valley and were never de- posited there. The Potsdam sandstone and the passage beds (Theresa formation) are also chiefly confined to the eastern sec- tions, though their thinned edges appear in the easterly Mohawk sections. The Chazy is absent in all sections, the Iowguiilemios some even younger) limestone resting on the Little Falls, the Tribes Hill or on some later division of the Beekmantown, in the various sections included in the table. Stratigraphic positions of the Potsdam, Little Falls and Tribes Hill formations Saratogan series. Though the Saratogan was defined and is generally accepted as the name of the closing stage of the Cambric in America, it 1s now practically certain that the deposits of the series in New York are of a later date than ate the formations im Missouri, Texas, Oklahoma, Wyoming and elsewhere, that Walcott and others have referred to the Upper Cambric. While there can be no question concerning the essential equivalence of the beds in the latter states, as indicated by stratigraphic position and persist- ence of lithologic and faunal characters, the facts are altogether different in the case of the typical New York Saratogan. Prac- tically the same fauna, the species in many cases being identical, occurs in the middle and more western localities in America in beds corresponding to the sandstone and chert beneath the Jordan sand- stone of the upper Mississippi valley section. ‘These beds are fur- ther distinguished except, in the Great Basin, by the rather abundant presence of glauconitic-or chloritic grains and by the almost con- stant presence of thin limestone conglomerates in their upper parts. Apparently very general sea withdrawal occurred at the close of this Upper Cambric stage. So far as known this Upper Cambrie sea is scarcely represented in the Appalachian valley and certainly it did not extend into the middle and northern parts; but it spread widely in the median areas between the Appalachian and Cordilleran troughs. | The return of the waters introduced the proposed Ozarkic period of Ulrich. The: new sea differed greatly from the pres ceding Upper Cambric sea in that it failed to cover the Rocky mountain area and in that it submerged the Appalachian and more SIXTH REPORT OF THE DIRECTOR I9QOQ 131 inland troughs and basins to Canada. In the Mississippi valley and in central Texas its deposits cavered about the same areas previously held by the late Cambric sea. It is this Ozarkic sea that rather early in its history surrounded the Adirondack uplift, laying down first the Potsdam, then the Theresa and finally, when conditions had become fairly quiescent and estab- lished, the Little Falls dolomite. However, long before the close of the Ozarkic the waters were again withdrawn from New York into reconstructed Appalachian troughs, remaining also in the but slightiy modified basins of the Mississippi valley. The more essential features of the evidence on which this interpretation is based may be briefly stated as follows: (1) The stratigraphic relations of the Potsdam to the Theresa and of fae to the Little Falls indicate a practically uninterrupted sequence of sedimentation. There was gradual reduction of adjacent land areas, and there may have been slight oscillations, but there is no evidence of a break in deposition nor of change iets character that may not be explained as of purely local significance. (2) So far as known there are no deposits cor- responding in age to the Upper Cambric in the Milississippi valley in areas intervening between this valley and the Adiron- dack region; neither have any been discovered in the middle fae Or the Appalachian valley nor in the Atlantic province; hence there is no means of directly connecting the Potsdam- Little Falls deposits and faunas with true Upper Cambric life and sediments elsewhere. (3) The Potsdam and Little Falls are clearly recognizable in the Allentown formation (Ulrich) in central and northeastern Pennsylvania and in the lower and middle divisions of the Knox farther south in the Appalachian valley. The Allentown rests on Lower Cambric, both Middle and Upper Cambric being absent in its area. The probably equivalent Conococheague formation of the Cumberland valley in southern Pennsylvania, contains a Saratogan fauna but differs lithologically and is underlain by two Middle Cambric forma- tions. The lower Knox is underlain by a thin Upper Cambric, considerable Middle Cambric and some Lower Cambric, the southern Appalachian Cambric section being relatively com- plete. Each of these Appalachian Ozarkic formations is over- lain by from 1000 feet to 4200 feet of Canadian (emend. Ulrich) limestone and dolomite, represented in eastern New York by the Beekmantown. (4) The fauna so far discovered in the Sara- 132 NEW YORK STATE MUSEUM togan of New York, particularly in the Hoyt limestone, is en- tirely distinct from that found beneath the St Lawrence lime- stone in the upper Mississippi valley, but some of the species occur there in the overlying calcareous and arenaceous deposits (St Lawrence limestone, Jordan sandstone and Oneota dolo- mite), while all of them are included in the large molluscan and trilobite faunas discovered by Ulrich in the middle divisions of the Ozarkic in Missouri. Most of them occur there in the Gas- conade chert, which is the third from the top of the seven formations into which the Ozarkic in Missouri is divisible. All of these formations succeed the Bonneterre limestone and Davis shale, which carry the St Croix and Reagan fauna that is so widely distributed in the Mississippi valley, in the Rocky mountains and in Texas, and which Ulrich, chiefly on diastrophic grounds, regards as marking the closing stage of the Cambric in Amer- ica. If this is not conceded then there is no sufficient reason for drawing the upper boundary of the Cambric system beneath the top of the Ordovicic — which would go back to Sedgwicks’s original conception of his Cambric — nor for recognizing more than a single system in the Neopaleozoic, another in the Meso- zoic and a third in the Neozoic. If the Devonic is recognized as a system distinct from the Siluric on the one side and the Waverlyan on the other then the Ozarkic is no less. distinct from the preceding “‘Cambrian” and the succeeding Canadian system; and the Canadian is equally distinct from the Ordovicic. If the criteria relied on are deemed sufficient in any of these instances then they are equally sound and worthy of considera- tion in all the others. The boundary between the Cambric and the Ozarkic as here > drawn is everywhere recognizable and the contacts between the Ozarkic and the Canadian, and between the Canadian and the Ordovicie are likewise definite. This is because they are de- termined by diastrophism. But no one has yet succeeded in drawing a satisfactory boundary between the upper limit of the range of “© Cambrian” trilobites and the lower limit of ihe “ Ordovician’ gastropods and cephalopods. In fact there is no such boundary, since the latter were well established before the middle of the Ozarkic, and Cambric types of trilobites sur- vived through the Ozarkic into the Canadian and a few even into the Ordovicic. Of course, neither the beginning nor the closing deposits of these Eopaleozoic systems are even approxi- SIXTH REPORT OF THE DIRECTOR I9QOQ 133 mately similar in geographic distribution. There was too much oscillation for that. Indeed, it is only here and there within the great Appalachian and Cordilleran troughs that anything like a complete sedimentary record of any one of the systems is found. But these inequalities of distribution are an aid rather than a hindrance in the recognition of the boundaries, because they make them correspondingly more distinct where the breaks in the “record are expanded. The faunal distinctions marking the revised systems also are more definite and more readily apparent than are those hitherto relied on in discriminating between the Cambric and the Ordo- VICIC. In the trilobites and the brachiopods we use specific rather than generic types in discriminating between the Upper Cambric and the Ozarkic; likewise among the previously established conical and involute gastropods. The correlation value and use of such long-lived types is precisely as in the case of genera common to two or more of the later systems in whose discrimination, more- over, specific differences comprise a greater and greater propor- tion of the competent organic data. The surviving Cambric trilo- bites and brachiopods have then essentially the same significance in stratigraphic taxonomy that we accord to Spirifer and Atrypa, which are well developed in the Siluric and continued their exist- ence into subsequent periods; or to genera of Ordovicic trilobites that are nearly as well represented in the Siluric. To disregard the probability of transgressions of generic types from the earliest Paleozoic system into the next younger system is to stand in the way of progress in stratigraphic correlation and classification. The principle is recognized in the discrimination of all the later systems, why not also in the case of the American Cambric? The past practice of classifying, often without regard to stratigraphic evidence, all formations as Upper Cambric that are younger than Middle Cambric and apparently older than beds con- taining supposedly indubitable Ordovicic fossils, was possibly justi- fiable, but only so long as the faunal history of a great intervening mass of rocks remained to be accounted for. Now, however, since this old “ Calciferous ”’ hiatus has been peopled with a large mixed “Cambrian ” and ‘ Ordovician ”’ fauna, and since we have come to understand the stratigraphic relations of most of the formations concerned in the inquiry, some other arrangement that will express the facts is desirable. We need a vehicle that will permit us to cor- 134 NEW YORK STATE MUSEUM rect the misapprehensions into which the former terra imcogmita and our blind reliance on unsupported fossil evidence led us; a means of showing, for instance, the true stratigraphic relations of the Sara- togan fauna as developed in New York to the Upper Cambric faunas in Missouri and Texas, or of the Dictyonema filabelli- forme and the Tetragraptus zones, or the Tribes Hill and other Canadian formations to the Saratogan and later Ozarkic formations on the one side and the typical Ordovicic formations on the other. It is believed that the revised classification proposed by Ulrich ac- complishes this aim. The table given on page 129, though in- tended to show only the relations of the New York formations dis- cussed in this paper, gives a fair general idea of the proposed scheme. | Perhaps the most practical feature of the revision of the Eopale- ozoic systems, so far as the use of fossils in their separation is con- cerned, is that we can say that the cephalopods and the coiled gas- tropods, also true cystids, became prominent for the first time in the Ozarkic, that the true graptolites, true ostracods, true Orthidae and the Asaphidae are first seen in the Canadian, and that the tabulate and rugose corals, the cyclostomatous and cryptostomatous bryozoa, the pelecypods and the crinoids are well developed in the Ordovicic but unknown beneath this system. In short, the new arrangement is in accord with, and makes available in the broader stratigraphic correlations, the apparently definite vertical distribution of many im- portant organic types. This distribution has not been considered as it should be in the prevailing indefinite arrangement of the Eopaleozoic rocks. As hitherto conceived the cephalopods and gas- tropods, the Asaphidae and Orthidae, and the graptolites appear at undetermined stages in a “ Cambrian” system that has no more pre- cise top than the fortuitous first appearance of certain fossil types, arbitrarily assumed to be Postcambric, above a similarly indefinite upper limit of certain Cambric genera of trilobites and brachiopods. Obviously, there has been no uniformity of practice. Walcott extended the lower system as far up in the section as he could recognize certain Cambric genera. Others, with the laudable but insufficiently considered intention of fixing the boundary at a well defined stratigraphic break, went farther and drew the top of the Cambric at the base of the St Peter, while others with a similar intention extended the base of the Ordovicic down to the first break beneath the introduction of the cephalopods and coiled gastropods, that is to practically the base of the Ozarkic. More commonly, SIXTH REPORT OF THE DIRECTOR I9OQ 135 however, in areas containing Ozarkic and Canadian deposits the boundary between the Cambric and the Ordovicic has been left undecided, or it was drawn arbitrarily in the midst of what was thought to be a great, sparsely fossiliferous, transitional series of dolomites and limestones because its basal part contained surviv- ing remnants of the Cambric fauna, and its uppermost ledges held fossils too much like Ordovicic species to be interpreted otherwise than as Postcambric. This inharmonious practice was perhaps excusable under the pre- vailing state of knowledge concerning Eopaleozoic history. So long as the oscillatory character of the continental seas of this era and the consequent variable localization of their deposits were not ap- preciated, the formations occupying apparently similar stratigraphic positions had to be correlated, and the observed differences in their respective lithologic and faunal aspects were of course only geographic changes or merely local phases. ‘There was also con- siderable excuse for individual difference of opinion as to which of the organic and physical criteria were the most deserving of confidence. But now, since it has been learned (1) that the Presaratogan deposits in the Appalachian and Cordilleran troughs attain more than sufficient thickness, and that their diastrophic history in America fully satisfies the requirements of an ideal geologic system ;' (2) that the great deposits of dolomite, limestone and sandstone which usually succeed the Cambric were not laid down in a continuous broad continental sea, hence that the magnesian limestones at one place may be altogether younger or older than those at another; (3) that these dolomites, limestones and sand- stones are divisible or may be grouped into two distinct series, largely independent in geographic distribution and each character- ized by its own physical and faunal development; (4) that each of these two series attains an aggregate thickness of over 4000 feet of calcareous deposits, hence, that each is comparable in time value to most of the systems now recognized; (5) that their independence, first suggested by diastrophic and faunal evidence, is now firmly established by the actual superposition of 4200 feet of Canadian dolomite and limestone in central Pennsylvania on fully 2000 feet of Ozarkic deposits; (6) that in the Appalachian region the whole —< *On questionable grounds, discussed elsewhere by one of the present authors, Schuchert [Geol. Soc. Am. Bul. 20:513-22, 600-2] divides the Same interval into two systems (Georgic and Acadic). 136 NEW YORK STATE MUSEUM of the Canadian underlies an aggregate thickness of nearly 4500 feet of Ordovicic limestone; and finally (7) that essentially the same cycles of movement, of submergence and emergence, as are used in distinguishing four Neopaleozoic systems, also obtained in the Eopaleozoic and suggest the propriety of a similar division of the Eopaleozoic into four systems instead of two as heretofore. In view of these facts we ask: Is the present indefinite separation of the Eopaleozoic into Cambric and Ordovicic a reasonable and ade- quate classification? Are these divisions coordinate in rank with the Neopaleozoic, Mesozoic and Neozoic systems? Our answer to these questions 1s clearly anticipated in the foregoing comments and arguments. | Age of the Tribes Hill formation. A few words remain-to be added respecting the age of the Tribes Hill. The formation is certainly Postozarkic, but its position in the Canadian is less easily determined. Except that we know the formation to be unconform- able on the Little Falls and that the contact represents a consider- able hiatus, we have only organic criteria to guide us in determining the age. That the Tribes Hill is younger than any known Ozarkic formation is satisfactorily shown by the presence of Asaphus and three or four other trilobites that are wholly unknown in Ozarkic faunas. The same is true of the Ritbeirias; and the Dal- manella? wemplei1 also is of a type that has not=beem observed beneath the Canadian. With the exception of Eccyli- omphalus multiseptarius, the testimony of the gastro- pods is less positive, very similar, though specifically distinct, forms being found in Ozarkic faunas. The gastropods described by Cte- land from the upper chert zone of the Little Falls dolomite at Little Falls are clearly Ozarkic types and hence are not referred to in this paragraph. | That the Tribes Hill is Canadian (emend. Ulrich) is unquestion- ably indicated by its fossils; and the same evidence is almost con- clusive in assigning the formation to an early stage in this period. With the possible exception of an orthoid shell, all the species so far discovered in the Tribes Hill are distinct from those described trom the Beekmantown in the Champlain valley. They impress one as older. This suggestion is confirmed when we compare the Tribes Hill forms with faunas found in the Canadian in central Pennsylvania. ‘The nearest facies —there are at least five and probably six identical species — is found in the Bellefonte, Pa. sec- tion about 3700 feet beneath the top of the Canadian. None of the succeeding faunules in the Bellefonte section are closely allied. PaCS AN Oe ERIC Dt lS iS Ky SIXTH REPORT OF THE DIRECTOR I9Q0Q 137 Relying on the fossil evidence just given it seems almost certain that the Tribes Hill is at least as old and probably is older than the dove limestone in division B of the Champlain “ Calciferous.”’ This conclusion finds further good support in the fact that Cryp- tozoon steeli, the principal fossil of division B, is found in Pennsylvania above the Stonehenge limestone which there contains the Tribes Hill fauna. Oscillations of level As detailed work has been carried forward in northern New York during the past few years, the evidence has been steadily accumulating to show that with a possible exception during the late Ordovicic the Adirondack region remained steadily as a land area, being sometimes an island, at other times part of a much larger land. It appears further that frequent and often very local oscillations of leve! effected modifications of its shore line; that the present erosion surface cuts the rocks in such wise that the surface exposures are chiefly of the thinned, near-shore margins of many of the formations; that gaps in the succession are frequent, and with much variation from place to place; and that, because of these conditions, the New York section of these rocks is very thin and very imperfect. From time to time Cush- ing has summarized our knowledge of these oscillations.*. With each onward step in the detailed work, however, evidence of further, and unexpected oscillations appears; and no doubt we are, even now, acquainted with but a small proportion of them. Nevertheless our present understanding of them should be sum- marized. To begin with, no part of New York was submerged during the Cambric. Lower Cambric deposits do occur locally within the eastern edge of the State south of the Champlain valley but it is highly probable that these are masses originally laid down in a trough farther east and which were subsequently thrust westward to their present position. The somewhat doubtful Middle Cambric sediments found in Stissing mountain near Poughkeepsie probably owe their present location to similar thrusting. True Upper Cambric (St. Croixan) rocks are entirely unknown within the State. Neither have such been found to the *N. Y. State Mus. Bul. 77, p. 51-65. N. Y. State Mus. Bul. 95, p. 386-04. eo. Soc. Am. Bul. 19:175-76. 138 NEW YORK STATE MUSEUM east in the New England States, nor to the west as far as Michigan and Indiana. They seem to be absent also in the Appalachian folds north of Virginia. Evidently New York formed part of a very large land area during the Cambric ages. The first important and unquestionable Paleozoic submergence of the southern flanks of this land occurred in the early part of the sticceeding Ozarkic period. This was the Potsdam or Saratogan sub- mergence. Potsdam deposition commenced in the Champlain trough, toward its northern end, working southward in that trovgh, and also working westward up the St Lawrence trough. In its lower portion it was probably a continental deposit, but the upper portion carries a marine fauna, and this continues on through the passage beds into the Little Falls dolomite which lies directly above. The deposition was continuous and tn- broken, so far as we know, from the one formation into the other. The subsidence in the St Lawrence trough reached as far west as Kingston during the Potsdam and probably but little farther. From Kingston it extended southward at least to some point in the valley of Black river. To how large an extent western New York was submerged we do not know positively. It seems likely, however, that a considerable expansion of the upper St Lawrence trough occupied the north central part of the State and probably covered also the western part of New York and the central part of Pennsylvania. For various reasons which can not be discussed at this time, it seems unlikely thatetiae western lobe of the Saratoga sea connected with the eastern or Champlain lobe across the southern part of New York prior to the closing stage of the Potsdam. In this and the transition stage the highly emergent parts of the Adirondack uplift which now became an island, had been much reduced by erosion and gen- eral subsidence; and the supply of clastic matter consequently was much less during the succeeding Little Falls dolomite stage. However, just preceding the latter, warping occurred which caused reemergence of the northern and western flanks of the island and restriction of the sea to the Champlain trough on the east and the Mohawk basin on the south. The latter ex- tended southward to northern New Jersey where its deposits are recognized in the lower part of the Kittatiny dolomite; and thence in a southwesterly direction through central Pennsylvania. Gastropod faunas found at Beauharnois near Montreal, near White- SIXTH REPORT OF THE DIRECTOR IQO0Q 139 hall, N. Y., in central Pennsylvania and in northern Virginia, leave little doubt that this sea extended down the western side of the Appalachian valley to the Mississippi valley where the same species arte found in the middle formations of the Ozarkic system. A thinned edge of the upper Potsdam runs westward into the Mohawk valley, but thins out to zero rather rapidly, letting the Little Falls dolomite down on the Precambric. It is thought that along the Mohawk line the Potsdam shore had a southwesterly trend, or rather a trend more to the south than the present Pre- cambric margin, the two meeting at an angle; east of the meeting point the Potsdam appears underneath the Little Falls, while west of it the Potsdam is either absent or erosion has not yet cut down to it. This involves the assumption that the Little Falls subsi- dence covered more of the southern part of the old land area than did the Potsdam, so that, within the Potsdam zone there would be a strip of territory with the Little Falls resting on the Precambric. In some localities there is direct evidence that this actually oc- curred, and it was likely true of much of the southern and eastern parts of the Adirondack border. In the Thousand islands region we find merely the thinned edges of the marine Potsdam and Theresa formations with no sign of the Little Falls dolomite. However, since these were laid down in the extreme westerly portion of the St Lawrence trough it is theoretically possible that their deposition occurred while the dolo- mite was being deposited along the Champlain and Mohawk lines. But there is no positive evidence that such a condition obtained. On the contrary, according to the trend of the scant faunal evidence and the probabilities suggested by general disastrophic considera- tions the lower or typical Theresa on the west flank of the Adiron- dacks is essentially contemporaneous with the transition beds on the east side; and deposition was prohibited by emergence on the west side when the Little Falls was being laid down in the Champlain and Mohawk valleys. Following the Little Falls deposit, warping and differential up- lift ensued, causing the shore lines to retreat from the district and resulting in the unconformity at the top of the Little Falls. There was some wear also since the summit is uneven and the Tribes Hill rests on different beds of the Little Falls; and, the returning waters assumed a different arrangement, with a more diversified shore line. Beekmantown depression commenced with the Tribes Hill de- 140 NEW YORK STATE MUSEUM posit, which nearly everywhere in the Mohawk valley rests on the Little Falls. In the Black river valley, where the Little Falls is absent, it rests on the Theresa formation. It is absent at Middle- ville and Newport, in the West Canada creek valley, showing that there, at least, it did not extend as far northward on the Adiron- dack oldland, as the Little Falls did. It is absent also at Saratoga, indicating that there also we are beyond its shore line. The exact equivalent of the Tribes Hill seems not to occur in the Champlain valley. At any rate its peculiar fauna has not been observed there. Apparently it is older than the fine grained limestone of division B with which the revised Beekmantown begins in the Champlain val- ley. Judging from the evidence now available the Tribes Hill submergence formed a geographic pattern quite different from that of the preceding Little Falls sea. The latter covered the southern and eastern flanks, the Tribes Hill occupied more limited embay- ments on the southern and western sides of the Adirondack area. The depression at the west was short-lived, uplift following with in- creasing eastward tilting, giving rise to long continued submergence of the Champlain valley. By the close of Tribes Hill time the up- lift involved all the Mohawk region proper, the remaining divi- sions of the Beekmantown limestone being confined to the Cham- plain valley trough and its northern and southern prolongations. The upper Beekmantown is found to the north in the Ottawa valley. To the south Beekmantown deposits are recognized at intervals through southeastern New York, New Jersey and Pennsylvania. Although the Beekmantown is of extraordinary thickness in the last state (2000 to 4200 feet) even the thickest sections still indi- cate occasional interruptions in sedimentation and probably with- drawal of seas. At the close of the Beekmantown uplift again occurred, producing © the unconformity between it and the Chazy, in the Champlain valley. We have evidence also of a number of hitherto unsuspected os- cillations of the general region during the succeeding Black River and Trenton times. Since, however, we are here concerned chiefly with the lower formations, those are left for discussion elsewhere. +, & SIXTH REPORT OF THE DIRECTOR 1909 I4l eee SYMMETRIC ARRANGEMENT IN THE ELE- mens OF THE PALEOZOIC PLATFORM OF NORTH AMERICA! } BY RUDOLF RUEDEMANN We wish to present certain facts indicating that the structural development of eastern North America has taken place in such a fashion that a notable symmetric arrangement of its elements has resulted. This arrangement becomes espectally distinct when the large area of Paleozoic rocks extending from the Canadian protaxis south- ward is considered by itself. This area, which is roughly bounded on the west by a line connecting the head of Lake Superior with the Ozarks and on the east by a line inclosing the Adirondacks and Appalachia, we may for convenience term the Paleozoic platform of North America. It corresponds in its relation to the Canadian shield with that of the “Russian platform” of the European geologists to the Baltic shield. A glance at the geologic map of North America will show that this platform is a direct southward continuation of the Canadian shield or protaxis and bounded by southward converging lines that are direct continuations of the boundaries of that shield? [see chart II, where the line M-N indicates the southern boundary of the Canadian shield A}, as described by Suess and Willis. In the west the platform, like the Canadian shield, is separated from the Rocky mountain area by the north-south transcontinental depression that extends from the Gulf of Mexico to the mouth of the Mackenzie river and is occupied by Cretaceous and Tertiary rocks. Chart II shows that the Canadian shield and its Paleozoic platform together form a body strikingly similar in its outlines Sentmie whole continent, a fact that can not but suggest that the “Leitlinien”’ of this large epeirogenic element and the whole continent stand in genetic relationship. *Submitted April 1900. *The Mesozoic and Cenozoic embayment of the Mississippi Valley is, in this discussion, left out of consideration, because of younger age; like- wise the belt of Carbonic rocks to the west and southwest of the Ozarks, that forms the outer slope of the western arm of the platform, roughly corresponding to the area of metamorphic rocks on the opposite slope of the other arm, and properly belonging to the transcontinental depression. I42 NEW YORK STATE MUSEUM In comparing the sketch map, chart I with the diagram [chart III] in which separate shading brings out the elevated and depressed regions, it is seen that on either side of the Cana- dian shield or protaxis [A], there stand out, like cornerstones, two separate Precambric areas, the Isle Wisconsin [D,] and the Isle Adirondack [E,] in quite symmetric positions. Each has its extension connecting it with the protaxis in symmetric posi- tion, that of the Isle Wisconsin being directed northeast (partly submerged by Lake Superior), that of the Isle Adirondack north- west. From each of these extensions there runs outward, along the margin of the shield, a deep depression, the Lake Superior basin [D,] and the St Lawrence basin [E,]. The latter is less distinct through the disturbing influence of the Appalachian folding and probably much obscured by extensive overthrusting from the southeast along “Logan’s line.” The effect of Appa- lachian folding by crushing in one side of the symmetric structure here set forth, will be discussed more fully in another chapter [see p. 145.] From each of these cornerstones there extends southward like an arm, a broad belt of Precambric and early Paleozoic rocks, nearly the full length of the continent. The western arm can be traced by the great southward extension of the Precarbonic rocks of Isle Wisconsin to near the neighborhood of Burlington, the Siluro-Devonic inlier along the Mississippi above its junction with the Missouri and the large Precambric-Cambro-Siluric inlier or uplift. of the Ozarks in Missouri and Arkansas? [ D,]. Its “ Leitlinie” is shown in red overprint in the line passing from D, through D,.. Lhe eastern arm] ,—F..| has beenvbadly woven. ridden, broken up and forced inward by the tangential pressure that has produced the Appalachian folds. It is, nevertheless, still easily recognized in the belt of Precambric and Precarbonic rocks, extending south and southwestward from New York as far as Alabama. The two arms have later been somewhat disturbed and ob- scured, especially the western one, by the breaking down of certain portions south of Isle Wisconsin, where the Carbonic 1The Ouachita mountains in Arkansas probably represent, according to Dr Ulrich’s description [in Preliminary List of Papers, Am. Geol. Soc. 21 Meet. 1908, p. 21] and as already indicated by their strike, a different element and will, for this reason, be left out of the discussion for the present. Ey eit Oe Dei 4 ary’ Ea a ” ” een Re eh, ee ede ~~ P} eee e : \ ‘ fam ae bien: wee — = 1 F ' aR | UU . - , , MeV ivennne,.. H ri “ , E % ein ; #30) he, 4 wot 7 if aap an ee fs ; sil! ' Do i \ t J : os & eS >. “SS ran A ik ae . jem a. 4 7 — 7 oi } 4 mr Ach i eh Na i ek i NA UE a Ts Vf we kia 4 ee ene ; LN ergs ert ¢ 2 is \e @ rein tte Teal tae ae ecg bog md el YY Feces ee aad bbe * : di Let i mane OF the eh O, pdgei) brady yilsye ViFapotsrn Ay aidt \4 Gh valzek) iat Gh ciret peat 6+) 7 g ; ‘ie : APE MARIE TH, Sehnan. vo Dy a) conan gi , Sens Cy Or Ab ree . os wt. > % ne i ee in ap ew ng ¥ A ta ty apnnrsp een prema ne at } Ooty Sa) nee Pressions of the shield, D,-D, guide line of western arm of platform. line of axis of eastern basin, to GEOLOGICAL SKETCH MAP OF THE EASTERN UNITED STATES MN southern boundary of Canadian shield A. Dy and Ey the symmetric Isles Wisconsin and Adirondack. D,; and E, the adjoining marginal de- B, Cincinnati geanticline. B, Michigan basin. E,-E, that of the eastern arm, Dg Isle Ozark. Eg Isle Appalachia. B, and By symmetric subbasins B,-B, guide — ALA AAS Precambric Algonkic Metamorphosed Paleozoic Cambro- Ordovicic GY Siluric WLLL Devonic z Mississippic Pennsylvanic | ee ee ney ~ = uf « Poh Weer skeen a RINT 1 i 4 . 2S ‘ boo it ; a : Tile Dati += ‘ . ; j fer eee ae { % ' ae * a si % 4 ‘ i a ee x ( ; 4 Oe ae i f / ’ a on t r be \ Le y say ‘ ' j Fale ; ch 4 , ( hid SAMO oe v a f i a 1U, 4 ens arg \ bod i ee P, aS i¥ re} : aN ¥ 1 L a = CAP ‘ df ~ 7 4 re - t ry ey (yet Wy ? ‘oY ¢ rut fue o be adalat F cp CT 4 niy cto ‘ nd \ ree tT abbiiey T7) way ghh” 3Ps SIXTH REPORT OF THE DIRECTOR I90Q 143 has transgressed it, and the eastern one by the submergence of portions southeast of the Adirondacks and by extensive fold- ing. In their original position the two arms may be conceived as approaching each other somewhat in the south, although not nearly so much as they do now, in consequence of the forcing inward of the eastern arm, for if the considerable shortening of the Eastern basin indicated by the Appalachian folds, is taken into account and the basin spread out to its original width, the eastern arm would probably take a position fully corresponding to that of the western. These two arms bound a large basin !B of chart II], the “ Paleozoic eastern basin,” now occupied by the basin of Ohio and the Great Lakes. In the middle of this an elongated low eleva- tion formed, now indicated by the Cincinnati and Nashville “ up- hehe. The axial position of this uplift [see lime B,-B, on chart I] suggests that it may partake of the nature of the “ geaniticlinal median ’’? that according to Haug? forms along the median line of a geosyncline preparatory to more extensive folding. The southern portion of the uplift which according to its normal posi- tion to the basin and the Precambric arms, should extend due south, has been affected by the Appalachian folding and twisted into a southwest direction. As a result of the warping of the axis of the basin, two separate symmetric basins have been formed,* one, the Eastern Interior, and the other, the East Cen- tral basin. On account of the approach of the Precambric arms in the south, these basins dc not extend north and south, but extend symmetrically to northwest and northeast. The Ohio river from the Pennsylvania to the West Virginia line flows along the axis of the eastern basin. The northern portion of the Paleozoic platform that lies to the north of the Cincinnati geanticline assumed the aspect of a separate subcircular basin, typically indicated by the Michigan coal field and the locations of Lake Michigan and Lake Huron. It also *Dana clearly recognized this uplift as a geanticline. aelage @mile. Soc. Géol. Fr. Bul. 28, ser. 3. 1900. p. 617, and id. Traité de Géologie I. 1907. p. 164. *Dana [Areas of Continental Progress in North America, etc., Geol. ~ Soc. Am. Bul. 1890. 1:41], recognizing the importance of the regions of shallow seas represented by the Cincinnati uplift and the Precambric region of Missouri as regards rock-making, has distinguished these basins by the terms here used. 144. NEW YORK STATE. MUSEUM lies symmetric to the whole arrangement and with the Cincin- nati uplift it is on the line of symmetry. It is possible that this Michigan basin, instead of being an independent depression, originated from the same warping force as the Cincinnati up- lift, being the result of a longitudinal oscillation of the axis of the same geanticline, comparable to those more intensive longi- tudinal oscillations of the axes, which have been observed in some of the Alpine folds [see Haug, Traité p. 211]. The Cana- dian geologists, however, have claimed to find the influence of the Cincinnati uplift extending from the west end of Lake Erte further north to Lake Huron, In this:case it}wouldtseemmuni: the Atlantic pressure had affected the entire extent of the up- lift [see p. 145]. giving» it a direction subparallelito ime Appalachian folds, and the Michigan basin would have to be considered as independent of the Cincinnati uplift, a view distinctly _ not supported by the general distribution of the formations around the basin. The development of these symmetric structures may have taken place as shown in charts IJ and III. Jn chart JI the Canadian shield A and its Paleozoic platform are outlined, the two sep- arated by the line M-N. First then, an extensive depression affected the middle portion of the platform producing the Paleo- zoic eastern basin B, and leaving two long embracing arms standing, the western one D and the eastern one Hai siteme depression had also taken place in the northern slope [C] which finds its expression in the ‘Hudson Bay embayment) ))Simce this and the eastern basin lie with their longitudinal axes on the same line (meridian), the idea that they may be expressions of the same warping movement, is worthy of some consideration. In its favor could be mentioned the fact that a path of migration is postulated along this line for the Niagaran fauna by Weller and a Devonic’ embayment by Schuchert. It will be noticed [see chart II] that the Hudson Bay Devonic embayment [C] and the Michigan basin approach so much that only a relatively narrow Precambric belt separates them, upon which, moreover, still a small Paleozoic outlier (n.e. of Georgian bay) remains. It is therefore quite probable that temporary depressions ex- tended there across the protaxis, and that the resulting Siluric and Devonic rocks have disappeared again by erosion. Chart III illustrates the changes which next took place in the two arms and in the inclosed basin. The arms were broken te Chart 2 RS NN VAAN BY ANS Sat Ve 63° 43 3. 23 13 ° 7 Diagram of the Canadian shield A with Paleozoic platform D B E. M N southern boundary of shield. C Hudson embayment. D western arm of platform, E eastern arm, B inclosed basin SIXTH REPORT OF THE DIRECTOR IQOQ T45 up, with the result that on either side two principal isles, Isle Wis- consin [D,] and Isle Ozark [D,], Isle Adirondack [E,] and Isle Appalachia [E,] were formed. These isles are distinctly paired. On either side between the Canadian shield and the first isle a de- pression formed, the Lake Superior basin [D,] and the St Law- rence basin [E,], and other depressions between the first and second isles. In the Paleozoic eastern basin a broad low anticline, the Cin- cinnati-Nashville parma [B,] arose,t exactly in the axial line of the depression and in continuation of this line of elevation the northern part of the basin sank down into an axial basin, the Michigan subbasin [B,]. On either side of the parma, between the latter and the Precambric arms, two basins, the Maer eweniral (6, and the Eastern Interior basin [B,] were formed, in such an arrangement that they converge southward and are exactly symmetrical to the axial line of the eastern basin. Chart IV illustrates the effect of the sub-Atlantic pressure, the cause of the Appalachian folding and overthrusting. This stress crushed or crumbled this symmetric structure from the southeast, its influence being felt in the whole eastern portion of the area. Following Claypole’s earlier estimates, Willis, [Geol. Soc. Bul. 1907, 18:404] remarks that “it is a moderate statement to say that during the Appalachian revolution that portion of the continent southeast of the Cumberland Plateau rim moved northwestward at least 50 miles.” ? On account of its oblique direction to the north-south axis of the Paleozoic eastern basin, the stress reaches deepest into the latter in the south, where it has clearly turned the Nash- ville portion of the Cincinnati-Nashville parma aside. It further *Suess has termed such broad warpings “ parmas.” *Dr Willis arrives at this estimate in the following way: It is well established that the folding of the Paleozoic strata in the Appalachian zone corresponds to a narrowing of the zone by 35 miles or more — that is, the Blue ridge approached the Cumberland plateau from a distance of 100 miles to within 65 miles. The general effect may best be de- scribed as a composite overthrust from southeast toward northwest. Keith’s recent investigations show that overthrusts of equal or greater displacement traverse the gneisses of the Smoky mountains. Hence it is a moderate statement to say that during the Appalachian revolu- tion that portion of the continent southeast of the Cumberland Plateau rim moved northwestward at least 50 miles. 146 NEW YORK STATE MUSEUM lengthened the Eastern Interior basin, and extended it into southeastern New York, or considerably farther north than the opposite East Central basin. Moreover, it may have produced secondary depressions east of the Michigan basin, which have finally found expression in Lakes Erie and Ontario. The prin- cipal facts suggesting the latter view are the general parallel- ism of these lake basins with that portion of the Appalachian folds southeast of them* whence the push came. It should, however, in this connection be taken in account, that it can have been but the last stages of Appalachian folding that produced the gentle down-warping of these basins, since the outwardly convex strike of the earlier Paleozoic formations (best seen at the west end of Lake Ontario) shows that this was an elevated re- gion until at least Devonic time. It is therefore quite possible that these depressions are the counterparts of the late (early Tertiary) domelike warpings in western Pennyslvania? and southern New York, to which their longitudinal direction clearly corresponds. 7 The joining of the Appalachian folds that die out in south- ern New York by a new north-south system of folds in eastern New York, brings the folded region close against the Adiron- dack isle and produces another depressed “ Vorland,”’ the Cham- plain basin. The Ottawa-Montreal basin that corresponds in its position and also in its form, in surrounding the north side of the Adirondack isle, to the Lake Superior basin, has also been much encroached upon by the westward pressure of the folded region and no doubt to no little amount by extensive overthrust. It will be seen that with the conception here presented of the geologic development of the eastern United States, the Great Lakes fall, by the first impetus to the formation of their basins —omitting the later accessory agencies, as glaciation and pre- glacial drainage-lines—into three groups, viz: a Lake Superior, originating from the breaking down of one of the arms of the Canadian shield.” *By drawing a straight line connecting the folds from the Tennessee- Virginia line to the Pennsylvania-New Jersey line, one obtains a line that indicates the general direction of this portion of the folds, and that line is parallel to the two lake basins. * See Campbell, M. B. Geol. Soc. Am. Bul. 1903. 14:277. *The Lake. Superior basin clearly antedates all the others, at least with its western arm which rests in Algonkian rocks that indicate a very early depression in the Canadian shield. re magne —_— | aa ' me ee eee ae H ‘ : * Sa i j } ( 2 i i ch i Lox aida c 4° . Diagram to show events on southern ing as on ' 0 Oe OS er een, Anet -me ed eRe | | | ® SR A A Res oe ees mew owe, | ie + a “ t = My ——— ate nen nett pcarsey (aaa eee, Ve t | | | i I aS ER ar Diagram to show events on southern sl Ae : | ae oe 4 \ ‘ eal ds Bs . Rete Hee 4 ts ae ein -<--~ See ie =A ee pes ecceencs eae 0 ope of North America still without interference of Atlantic pressure. chart 1. Arrows indicate main outlets of basin B. a U ~ we ¥ Ba Lettering as on Tee at ¥ ny ke ‘3 Pe a tera ee ae Re THe yt a Swerhawiaé- poled dre elo wgoke steals ardsitinaimigin oisothnt eworrA ”..1 “pipiog ik Fw" iain wie res cit in ine obtang: >» vue ie . '. 4 2 no eiaove wode of me Orth: sid SIXTH REPORT OF THE DIRECTOR I9Q0Q 147 b Lake Michigan and Lake Huron. Their location and form cornespond to the Michigan basin, where they roughly follow the Devonic belts. _ c Lake Erie and Lake Ontario, either depressions originating from the action of the Atlantic tangential pressure, or counterparts of later warpings in the upper Ohio basin and western New York. We have thus far left out of consideration the Appalachian basin or “‘ geosyncline” which occupies a narrow strip on the west side of Appalachia [chart IV] and is continued northward through New York and Vermont into Canada. It has later become the site of the Appalachian folds. Ulrich and Schuch- ert? have clearly shown that this basin became early subdi- vided by longitudinal and transverse barriers into a number of smaller basins. In their directions these barriers foreshadow the later, more intensive Appalachian folding, and are early indications of the influence of the pressure acting from the Atlantic basin upon and through Appalachia. It is certain that the Appalachian basin itself which became the site of the intense folding resulted from the Atlantic pressure upon Appalachia, due to suboceanic spread. It is therefore a foreign element, so to say, in the geologic history of the Palezoic platform which, however, has strongly obscured the original symmetry of the latter. While all changes here noted on the platform are of epeirogenic character, the Appalachian folds are an orogenic feature. While in general the isles have emerged in Paleozoic times and the basins have been submerged, there have been continuous changes in the amount of emergence and submergence. ‘This fact becomes especially manifest through Professor Schuchert’s paleo- geographic maps, as far as they have appeared in print, and it is probable that these subsidences and elevations took place in rhythmic pulsations. With all these continuous changes, however, the sum total of the elevations of isle Wisconsin, isle Adirondack, Ozarkia and Appalachia has been greater than that of the depressions and they represent, therefore, positive elements of the continent in the sense used by Willis? while the depressions are negative elements in which, however, in some zones, as in the Cincinnati uplift, the algebraic sum of the unconformities and sediments may approach zero. The most conspicuous negative element is the Appalachian basin with its immense sedimentation. ~ Saeee state Mus. Bul. 52. 1901. p. 633. “Willis, Bailey. Geol. Soc. Am. Bul. 1907. 18:38. 148 NEW YORK STATE MUSEUM The symmetry of arrangement of the platform is likewise but a surplus of symmetric features in the general structure over many asymmetric details in the different stages through which the platform has passed. This again is well shown by the charts of Professor Schuchert. It will be seen that at times the Nashville uplift was joined to Appalachia, and the Easter’ Interior basin moved northward, whiie the East Central basi was divided by a secondary peninsula (Kankakee) and Ozark’ joined to a vast western tract. But at the same time the t arms of the platform with their northern isles Wisconsin ° Adirondack (as peninsulas) and the southern land bodie: Ozarkia and Appalachia remained distinct elements ar ' wise the Mediterranean basin remained defined in its ; outline. i The main outlets from the Paleozoic [see chart IIT] eastward between the Isle Adirondack and Appalach westward between Isle Wisconsin and the Ozark upl southward between Ozarkia and Appalachia. The Wi and Adirondack isles have apparently been frequently al/. #™ to the protaxis. This becomes. especially manifest in t} of the Adirondack isle, where the Beekmantown, I>. Chazy, Lowville and probably also Black River format «1's not cross the connecting Frontenac axis. -The St Lawre pression, however, frequently became an important high .y of migration (as in Beekmantown, Onondaga and Hamilton times) through its southward connection, by different straits, at dif- ferent times with depressions between the Isle Adirondack and Appalachia [see p. e. Schuchert’s map of Onondaga time]. There are facts available that indicate approximately the time when the symmetric arrangement of the Paleozoic platform took place. As we have noted before, Algonkian sedimentation took place around Lake Superior [see chart I] but aside from this some- what independent depression, the whole platform was, according to Walcott’s investigations,' above sea level until Upper Cambric time, with the exception of the Appalachian geosyncline. The relation of the Upper Cambric deposits to the Isles Wisconsin and Adirondack would indicate that in this period the separation of the Paleozoic eastern basin and of the inclosing arms, took place and prob- ably also the beginning of the breaking up of the arms)? item Isles Wisconsin and Adirondack, Ozarkia and Appalachia have *See pl: 2, 3 ot Walcott: U.LS, (Geol Sur, Bul. om icon ep Cates ce + ae ow = + ~~ i aw eemens aS as ena aS a a - as Ve ‘ i * ? | —— \ Wp . 4 My —--- = kes the is It is Fis (paeradvmcnertem ae ben oats pamms swmmaunnnanaannaanns anne * ! ‘ ; \ ) a Diagram to show g Le ; 7 he ay ‘ ‘ee vats 1 oo é ‘ —_ Ze \ -- : q | aise | Sa ae * ‘ i * 4 I : t 4 ! . | . Let AN 4 \ Z \ ie t oe at Ol H a SS Le ‘ ase 2 ! ares | i > | 1 \ I \ j i \ Wh a i tf : ‘ : NLA | Pree cent scence ene EE i results of+ and geanticline Bu. te ha, i Se te i a a ce th a Ra i aaa — : Be teers Fe ar Ses Se oe i \ . 3 | | : | : 3 ) | | | : : kat ! i ; | | | i ' 3 : 2 : i D S \ t o* ; : t \ . : 7 4 U Gui Bes =<) eee : tact | OG oe : ‘ | a i es oy : : 5 . ras Aiden: b a 4 : a i ET) £l ai , Lh Wea i a erie Wes ; A / TT —,, ; out —\. r" , PPM hiss z ! } Anais | ( var Santee TS 10° s Diagram to show results of Atlantic pressure (indicated by arrows) on eastern arm E2-Fs, subbasin Ba and geanticline Bi. F belt of folding through Atlantic pressure 7 ~~ ee H aptedre tee petri nn wa on — a. & ~ Hbaeencas ae 1 Ast het naam eae ae eg ee eb pama' op aonsewtea Serna ec SIXTH REPORT OF THE DIRECTOR IQOQ I49 ‘remained above the sea since the end of-the Lower Siluric. In Upper Siluric time the Cincinnati parma had become a promi- nent feature, although the Cincinnati and Nashville parts of the same were again separated repeatedly, as in Hamilton and Mis- sissippian times, by the submergence of the middle part. In Carbonic (Mississippian and Pennsylvanian) times all the sub- divisions of the platform distinguished above, were fully developed. Since then the platform has remained land, with nee exception of the Mesozoic Mississippi embayment. Summary The writer endeavors to point out: 1 [hat the Paleozoic platform of North America extending south from the Canadian shield, forms, together with the latter, a structural element of the continent, that is similar in outline mothe latter. 2 That the Paleozoic platform exhibits a symmetric arrange- ment of its parts. This symmetric arrangement consists in the presence of a median basin (Paleozoic eastern basin) that is flanked on both sides by broad elevations, extending southward from the Isles Wisconsin and Adirondack which possess symmetric positions with reference to the Canadian shield. Ozarkia and Ap- palachia, the two remaining portions of elevations, hold like sym- metric positions. 3 The axial line of the Paleozoic eastern basin is occupied by the Cincinnati-Nashville parma and the Michigan subbasin. The former divides the Paleozoic eastern basin into two similar and symmetric basins, the Eastern Interior and East Central basins. 4 The disturbing factor has been the Atlantic pressure, which pushed the eastern arm in and produced the Appalachian basin folds, its effect reaching as far as the Nashville uplift. 150 NEW YORK STATE MUSEUM ORIGIN OF COLOR IN THE VERNON] SHARE BY W. J. MILLER 3 For over 50 years the subject of the origin of colors in rock formations has been much discussed and many explanations have been offered. Of the early papers that by Maw!’ in 1868 is perhaps the most able and comprehensive. In 1879 Julien? published a paper which contains a discussion of the origin of red formations. In 1899 Russell* ably treated the subject of subaerial rock decay and color origin in certain rocks. His paper gives a good summary of the views expressed by earlier writers. In 1908 Barrell* gave an excellent discussion of the origin of such colors in rocks. It is not the purpose of the present brief paper to deal with the phenomena of colors in rock formations in general nor to review the literature, but it is rather to confine attention to the color phenomena of the well known Vernon red shale of central New York. That the color phenomena in these shales are not merely superficial or due to recent atmospheric action, is proved by the fact that the same features have been found in deep wells passing through the formation. The Vernon shale has its type locality in the town of Vernon, a few miles west of Clinton, and it extends from southern Herkimer county westward across the State. Wherever exposed the shale presents a striking appearance due to its red color. A section, in- cluding the Vernon shales, near Clinton is as follows in descending order : 3 Camillus formation — Dark, thin-bedded shales c 5 feet of light green shale b 135 feet of dull red shale, unstrati- fied and with green spots scattered through the mass 10 feet of light green shale 1 Niagara formation — Dark shales and sandy limestones. Con- tains large concretions. The red shale, with the green bed at its base, is well shown in the ravine just north of Hamilton College and in Kirkland glen nearly 2 miles southwest of Clinton. The upper green bed, with the Camillus above and the red shale below, are well exposed at the 2 Vernon formation — | (150 feet). a reservoir 2 miles southwest of Clinton. At the “ Dug-way,” 2 _ *Geol. Soc. Quar. Jour. Lond. 1868. 24:351-400. 2 Am. Assoc. Adv. Sci. Proc. 1879, p. 311-410. °U. S. Geol. Sur. Bul. 52, especially p. 44-56. *Jour. Geol. 1908, v. 16, especially p. 285-94. SIXTH REPORT OF THE DIRECTOR I9Q0OQ I5.l miles south of Clinton, a 2 inch layer of green shale is locally present a few feet above the basal green bed. Scattered throughout the red shale are numerous green spots and after a shower the colors are intensified so that the light green spots stand out in sharp con- trast against the dull red matrix. The formation is everywhere highly jointed and soon after exposure to the weather the rock _ crumbles to a fine dust. The shale is very fine grained and, except for color, it is remarkably uniform from top to bottom. So far as observed it is entirely devoid of stratification planes. Thus it is evident that deposition of the sediment must have occurred in quiet water and under very uniform conditions. Except for cer- tain organic patches below referred to, not a trace of a fossil has been found in the formation near Clinton. At Syracuse the salt bed rests upon the Vernon shale and the absence of fossils from the shale is probably due to the fact that just before the real salt pan conditions the water was too saline to permit much, if any, animal life. | Origin of color in the red shale. The red shale is very fine grained, but examination of the powder or the thin section shows it to be made up chiefly of tiny quartz grains which are imbedded in a red matrix of earthy or claylike material. Occasionally small rhom- bohedral crystals of some carbonate are noticeable. Because of the opacity and softness of the shale thin sections are difficult to make but it is evident that the color is not inherent in the quartz grains which are themselves very clear and free from color. This is in harmony with Russell’s! observations on the Newark sandstones, that “their color was not inherent in the particles composing them, but was due to a fine, amorphous, claylike coating which enveloped the grains and filled the intervening spaces.” The red color is unquestionably due to the presence of de- hydrated ferric oxid. On treating the red shale with hot hydro- chloric acid the red color quickly disappears because the ferric oxid dissolves and from the solution a good precipitate of brown ferric hydrate is obtained by the addition of ammonia. Quantitative tests by Dr A. P. Saunders of Hamilton College showed that a sample of the red shale, treated with hot dilute sulfuric acid, contained 2.25% Of ferric iron and .75% of ferrous iron.2, The amount of ferric Sep. cu. p. 44. *The amount of ferric iron here given is doubtless greater than is actually present in the oxid form because the acid was boiled until it became concentrated enough to effect a partial decomposition of the green silicate residue below referred to. 152 NEW. YORK STATE MUSEUM oxid is thus very small, but, because of its fine state of division and its diffusion through the mass, it has become very effective as a coloring agent. Barrell’ discusses this point and believes that where even a very small percentage of the ferric oxid is thoroughly dif- fused through a rock mass it has great coloring power. It should be stated that after treatment with the hot acid a green insoluble residue is left, whose color disappears after prolonged boiling with concentrated sulfuric. acid. Under the microscope this green residue, whose color is doubtless due to the presence of glauconitic material, looks like the ordinary red shale except for color. ‘The final residue 1s made up chiefly of clear, tiny quartz grains. The relation of the ferric oxid to the glauconite could not certainly be made out but they appear to be very intimately mixed in the earthy matrix surrounding the quartz grains. The origin and significance of the glauconite will be taken up later. We may now inquire whether or not the red color was present when the shale was deposited. According to Russell’s? hypothesis, namely “that the sands forming the sandstones of the Newark system and other similar formations received their incrustation of ferric oxid (red) during the subaerial decay of the rock from which they were derived,” the red color was present at the time of deposition. Barrell? comes to quite the opposite conclusion, espe- cially with reference to red beds associated with salt and gypsum as e. g. in Nova Scotia, the Permian red beds east of the Rockies, etc. Like these red beds, the Vernon shale is also associated with salt and gypsum and was also deposited in rather highly saline water under an arid climate. As Barrell* says the lack of the red color at the time of deposition is well borne out by the “ usual present development of salt and gypsum in association with gray or yellow sediments.” He cites such examples as the Dead sea and the salty flats of the Great Basin of the United States. It is evi- dent that red or reddish brown colors greatly predominate in ancient iron-bearing formations, while the yellow tones, outside of the tropics, are much more characteristic of the modern alluvium. It is well known, especially as a result of the Challenger® dredg- OPS: Clie 2p 250; 10p. Cb. DiasO: ° op. cit. p. 290. SOP. Cita), 200,016 s Challenger Report on Deep Sea Deposits, p. 337 et seq. SIXTH REPORT OF THE DIRECTOR I9QO0Q 153 | ing, that red clay is now forming as a widespread deep sea deposit | particularly in the Pacific, but these clays are practically confined | to the neighborhood of volcanic regions and they are considered to | be due chiefly to the deposition of volcanic dust. Obviously this mode of origin will not apply to the Vernon red shale because it is a terrigenous rather than a deep sea deposit. Some red mud? is now depositing locally as in the Yellow sea and along the coast | of Brazil, but it is being derived from moist, tropical regions where | conditions are favorable for spontaneous dehydration of the ferric oxid. Such dehydration of ferric oxid under conditions of warmth and moisture is well known to account for the deep red color of | laterite, the soil so characteristic of the tropics, and which colors the river silts. The climatic evidence is opposed to such an origin of color in the Vernon red shale. Applying Barrell’s view, the iron in the Vernon shale was present at the time of deposition in the peroxid form, but hydrated and therefore not red, and the dehydration with resulting red color was largely due to great pressure and moderate temperature in the con- solidated and deeply buried sediment, since hydrated ferric oxid readily gives up its water under such conditions. This dehydration, combined with the finely divided and diffused ferric oxid, the writer believes accounts for the red color of the Vernon shale. Very commonly stains of yellowish to yellowish brown oxi of iron may be seen along fractures in both the red and green shales, and these are clearly due to the hydration of some of the ferric oxid since exposure to the weather. | Origin of the green spots. As already stated one of the striking features of the Vernon formation is the presence of numerous light green spots scattered through the dull red shales. So far as tested the material of these green spots is precisely the Same as that in the green shale beds in the formation. The spots Tange in size from a fraction of an inch to several inches in diam- eter. They are mostly spheriodal to flattened spherioda! and seldom irregular. When flattened the long axes lie horizontal thus sug- gesting that the flattening has been due to the pressure of overlying Strata and this since the spots were formed. The green spots are nearly always in sharp contact with the surrounding red shale but, *“Mud is a mixture of minerals in a state of extremely fine mechan- ical subdivision, but not chemically decomposed, thus differing from clay.” Scott’s Geology, 1907 edition, p. 267. The Vernon shale is essen- tially a hardened mud. 154 NEW YORK STATE MUSEUM aside from color, there appears to be no difference in character between the red and green materials. Although the spots are very irregularly arranged they are, nevertheless, pretty uniformly dis- tributed through the whole mass of red shale, and it is estimated that they make up less than 2% of the mass. Another fact of im- portance is the frequent presence of dark to black centers in the green spots. ‘Such dark centers which are particularly well shown in Kirkland glen, range in diameter up to a half inch and they are rarely concentric. A much lighter shade commonly extends from — the black center well out toward the periphery of the green spots. ~ These dark centers are certainly organic, the dark color being com- pletely removed by heating before the blowpipe. After treating the green spot material with hot hydrochloric acid a green glauconitic residue is left precisely like that from the red shale. Ferrous iron has gone into solution as shown by the heavy blue precipitate with potassium ferricyanide. Am- monia, however, fails to give the brown precipitate for ferric iron, while sulphocyanate gives only a slight coloration. This coloration is doubtless due to the fact that by infiltration a small amount of hydrated ferric oxid has comparatively re- cently been mixed with the green spots. Ferric oxid is, there- fore, practically absent from the green spots. According to an analysis made by Dr A. P. Saunders, a sample of the green spot material contained 1.19% of ferrous iron obtained from the dilute sulfuric acid solution. The writer believes that the ferrous iron is largely present in the carbonate form. Both the red and green shale when treated with cold hydrochloric acid show al- most no sign of chemical action but after warming a vigorous effervescence sets up and this suggests iron carbonate. This car- bonate doubtless forms the rhombohedral crystals seen in thin sec- tion. Many years ago Vanuxem! described these green spots and stated that: “It 1s not easy to resist the impressionmtiageere green color is the result of a change in the red particles, the peroxid of iron being reduced to a protoxid.’ He makes no mention of the black organic centers. His view is still com- monly held but there are certain objections to it as for example the highly improbable assumption that the red color was original and the fact that the chief coloring matter in the green shale is glau- conitic and not protoxid of iron. Qe i So Fr GEE, Me SSRI Lan a, I tg I Geol: 3d Dist.“ Na Yoo 18425 pacer SIXTH REPORT OF THE DIRECTOR IQGOQ 155 Maw, il reretting to green spots in general, stated that: “The generally accepted theory, and that suggested by De la Beche in explanation of the phenomenon, is, that the discolora- tion has been brought about by the reduction of the sesquioxid to a lower state of oxidation of less coloring power by simple chemical reaction with the fossil carbon.” The objections above given apply in this case also but the influence of the organic Matter is here clearly brought out. As early as 1831 Fleming? ‘recognized the agency of decomposing organic matter in the production of the light colored (but not green) spots in the Old Red Sandstone. It is well established that decomposing organic matter will effect the reduction of ferric to ferrous iron and the organic matter in the green spots of the Vernon shale has no doubt Sesed such a change, but since, in this case, the ferric oxid was in the hydrated state and hence not red, it is not correct to say that there was a change in color from red to green. Rather the writer believes that the presence of the organic matter has simply prevented the appearance of the red color in the immedi- ate vicinity because the oxid of iron has here all been reduced to the ferrous condition. Within the spots, then, the green color of the glauconite is allowed to come out, and it is this rather than the small percentage of iron in the ferrous condi- tion which gives the green color. In each case the size of the green spot has been directly dependent upon the amount of the decomposing organic matter. The presence of ferrous iron in both the red and green shales may be readily explained be- cause this iron is probably mostly in the carbonate form which would be pretty freely disseminated through the whole shale mass. Origin of color in the green shale. In view of the above state- ments the explanation of the origin of the color in the green shales, at the base and the summit of the red shale, becomes a comparatively simple matter. The character of the material in the green shale is, in every way, like that in the green spots and the explanation of the origin of the color in the spots may be applied here also. In this case, however, the organic mat- ter was probably more abundant or, at least, it was more finely divided and scattered through the mass so that all of the ferric mee, cil. p. 371. *“Old Red Sandstone” by Hugh Miller, quoted on p. 235. 156 NEW YORK STATE MUSEUM oxid in the green beds has been reduced and there the green glauconitic color appears throughout. In the same way the color of the green streak in the red shale, above noted, has~ been produced. — Regarding the origin of the glauconite in the Vernon shale the writer ventures to suggest that the conditions for its for-7 mation were very favorable such as the deposition of the fine) ferruginous sediments very slowly and uniformly at the su called “mud line,” in the presence of decomposing organic matter. Since the waters were rather highly saline and since” no trace of fossil shells has been found, it is conjectured that the organisms were plants of the seaweed type. It is well known, especially by the studies of the Challenger! expedition, that greenish glauconite muds are now forming in the presence of decomposing organic matter over considerable portions of the ocean bottom particularly near the borders of the continental” shelves. In the case of the Vernon shale there was an excess® of ferric oxid over that necessary to the formation of the glau-~ conite and the dehydration of this excess oxid, as above ex- | plained, has given rise to the red color of the shale. | In Kirkland glen an interesting example of the effect of mod-~ ern decomposing organic matter has been observed by the writer.” Along a joint plane for 6 or 8 feet the ferric oxid has been re-~ duced so that, for an inch either side of the joint plane, the © shale is green. This is thought to be a purely superficial effect — since the hillside is heavily covered with humus and surface waters charged with humic acids have traveled along the joint” plane thus causing a reduction of the ferric oxid so that the 7 green glauconitic color is brought out. iq ‘ SOPs ib. D0 305-01. : oa en oe a a a ere potemeee U ( 4 ~ Ss ~ a= = oe / t] { 4 Q al < ae & i f : [is Yf J i Gf Y Jiggy’ — —— 0 ‘ v —__ Sea eee AL, eee Suse EEL. 57 ABI Ec) a Ln Section along A-B of above map, showing structure and derivation of the fault block SIXTH REPORT OF THE DIRECTOR IQOQ 157 mee yVR) OVERTHRUST FAULT AT SAUGERTIES, NN BY GEORGE H. CHADWICK Canoe ‘hill, north of Saugerties village, Ulster co., is repre- sented on the Catskill topographic sheet as a dumb-bell ridge with the highway passing obliquely across the narrowed middle. ° It is surrounded by clay plains of Lake Albany age, along which, on the west and north of the hill, runs the West Shore Railway. The Canioe ridge is a part of the range of Helderberg limestone hills, known locally as the Kalkberg (pronounced collabarrack,— “Collar Back” of the map!), which here sags under the Albany clays, its summits rising as a chain of islands out of the plain. During a recent visit to this hill in company with the two gentle- men named beyond, the writer was impressed by the occurrence here of an overthrust almost identical with those in the Vlight- berg at Rondout [see van Ingen & Clark. Disturbed Fossiliferous Rocks in the Vicinity of Rondout, N. Y. N. Y. State Mus. Bul. 69]. Although it seems likely that this fault has been observed iby others, no reference to it now occurs to the writer, and a brief account, with diagrams, is therefore presented because of the con- spicuous nature of the faulting and the more ready accessibility of the locality as compared with the Rondout faults. The locality is in the first hill northeast of Saugerties depot, and not over a mile distant. The map [pl. 1] shows the road crossing the hill in the oblique valley determined by the fault. The village stone crusher, located at the corporation line, fur- nishes a conspicuous landmark for the visitor. Opposite this, on the east, a blind road leads under the hill. Various quarries and diggings [Q] add to the ease of study of the ledges which are everywhere conspicuous. The rock at 1, by the roadside as one turns into the crusher quarry, is much brecciated and shot through with calcite seams. It looks like upper Manlius, but no tossils were found. The brecciation is probably due to its lying in the fault zone. At 2, the cliff face behind the stone crusher, the limestone is hard, blue and vertical, with calcite veins and geodes. The fossils are Sieberella galeata, Favosites etc., of the Coeymans lime- stone. Passing across the highway to 3, where the Manlius would 158 NEW YORK STATE MUSEUM | naturally be expected, the rock is found to be a bluish impure § calcarenite with Leptaena rhomboidalis, unlike the } Coeymans and not so steeply inclined. This grades rapidly — downward (easterly) into a coarsely crystalline “ coquina” rock, catrying Spirifer cyclopterus, with etcemiciumaaae partings in the lower portion (at locality 4)— unquestionably the - Becrait. limestone. “Mr “Gole reports “Sp ime aeeoe ropleura abundant in the shaly limestone beiow this, along | the road at 5 and beyond, indicating the New Scotland. The rock at 3 1s therefore the lower Port Ewen, with which it fully accords. The basal bed of this, close down upon the Becraft, carries some chert nodules, as at Catskill. | The Becraft and Port Ewen have an almost unbroken out- crop northward along the ridge. A digging at 6 shows plenty of Aspidocrinus in the upper Becraft, and a gradual change of rock texture at the contact with the Port Ewen. The higher 7 layers of the latter begin to appear, and are decidedly shaly and ~ with oblique schistosity, as at Rondout. They occasion a slight depression and are not well exposed. Beyond them again are — harder layers, somewhat cherty, at 7, forming a slight ridge; they: carry Leptocoelia flabellites abundantly walse Spiriier cyclopterwus and are either the hiotesemzann Ewen (beds 22 to 26 at Rondout) or iowest Oriskany. In ap- pearance they resemble the Hudson valley “Schoharie grit.” The dip is steep and the surface of the highest layer has been largely uncovered in a road-metal digging at 8. Here only the talus is being removed and the rock face is untouched but bared. It is horizontally glaciated, and a striking feature of the polished surface is the occurrence of Taonurus cauda-—™ galli as lighter colored spiral patches resembling paint blotches. Polished chert nodules aiso appear prominently. Slightly exfoliated surfaces show the normal burrow structure of Taonurus, side by side with Spirifer murehise@ums and Leptocoelia. This is therefore undoubted Glenerie Oriska- nian and indicates a rapid loss in calcareous content in the few miles between Glenerie and here. Standing in this pit, one looks against the north end of the other (or fault-block) ridge, with its nearly vertical beds well shown in an old quarry cutting. The nearest rock, at 9, is New Scotland shale with beautiful and frail silicified fossils, such as are found in it at High Falls station on the Kingston & SIXTH REPORT OF THE DIRECTOR I909 159 Ellenville (O. & W.) Railway. These are wholly different in appearance from the silicified shells of the Oriskany, Port Ewen or Kalkberg limestones and are readily distinguished. ‘They come irom essentially shaly layers, are very delicate, neither thickened, coarsened nor iron-stained but often semitranslucent blue with the finest edges and markings sharply preserved. dhe transition to the Becraft and thence to the Port Ewen is completely revealed, with excellent collecting opportunities. At 10, the west side of the same quarry, it appears impossible to draw the Becraft-Port Ewen contact at a bedding-plane. The two rocks are perfectly continuous, only the change of fossils and the appearance of chert nodules marking the inception of the Port Ewen. This is unusual; a distinct bedding-plane separates them at Rondout, Alsen and Catskill. From to a red barn is seen to the south, under the west base of the hill. Mr Cole states that beds with many Homalo- notus vanuxemi, supposedly Oriskany or perhaps upper Port Ewen, occur from this barn southward, having a low west- erly dip. Returning along the highway, another big cutting at II shews the same fossiliferous New Scotland shales as at 9, and these beds are being excavated again at 12, here quite vertical to beyond vertical at the top. No attempt has been made to discriminate the Kalkberg limestone in the field or on the map, from the underlying Coeymans. The offset between the two halves of the hill is plainly evi- dent. Only the narrow highway separates outcrops as discoid- ant as Oriskany and New Scotland, or Port Ewen and Coey- mans, and this nighway is seen to lie in an oblique hollow across the hill having every earmark of a fault valley. Standing on the north of the road, say at 6, the fault piane is felt to be the hill slope on which one stands, dipping at a low angle to the west- ward and a steeper angle to the southward. The fault block is like the decapitated crest of this hill, slid westward and slightly downward for the space of two or three hundred feet upon the yielding surface of the Esopus shale (which makes the next ridge to the west beyond the railway), just as at Ron- dout. Of course, as a matter of fact, the slip took place under much overlying rock and the present forms are erosional. The movement was a true overthrust, not a landslide. One is tempted to inquire whether this is not a piece of the identical fault 160 NEW YORK STATE MUSEUM which appears at Rondout, and whether it is not also one with the similar horizontal overthrust described by Davis at Aus- tin’s millroad near Catskill [Folded Helderberg Limestones. Mus. Comp. Zool. Bul. v-.7, No. 10, fig. 3) and. 322i tiem like puzzling features (not yet worked out) in the Kalkberg at Alsen and Cementon, and finally with the great fault near Schodack Landing and southward along the Appalachian front into Georgia. The influence of such a plane, nearly hori- zontal but rising and falling in great gentle undulations, would affect a wide area (compare the Rome folio, in Georgia) and produce seemingly very irregular, disconnected and puzzling results, especially where it hades, as in this case and so often, considerably beyond the horizontal. If not one and the same plane, these instances must at least appertain to the same set of movements; the same) aie mess tending along the entire eastern edge of the folded Appalachians as a constant and normal feature. The recognition of this for our miniature Appalachian hills of the Hudson valley will as- sist the field worker materially and will rapidly multiply the known occurrences of this structure. The writer owes the opportunity for these observations to the Rev. Thomas Cole, Episcopal rector at Saugerties and an ~ acute observer of local geology, in company of whom and of Prof. J. W. Eggleston of Harvard the reconnaissance was made. SIXTH REPORT OF THE DIRECTOR 1909 161 fee aAVES OF VALCOUR ISLAND — THEIR AGE f AND THEIR ORIGIN BY GEORGE H. HUDSON Wherever the shore of Valcour island consists of the purer dolo- mite limestones of the middle Chazy beds, it has been penetrated, sometimes to considerable depths, by a number of small caves which owe their origin in great part to the solvent power of water. The majority of these caves seem to have had their beginnings in exposed joint or fissure planes, and as a rule they have closely fol- lowed them in their subsequent development. Such deviation as exists is expressive of a well marked tendency to develop vertically. The form is usually somewhat wedge-shaped with the apex of the wedge, uppermost, and in the smallest caves this edge may sometimes be seen to be working upward across a dipping bed without any ap- parent fissure or joint plane as a guide. If the small cave has penetrated to considerable depths the inrushing volume of water from a wave condenses the cave air and this in turn shoots out a smaller volume of water at the cave top with great velocity. These spouting caves lose the sharp upper edge of the wedge and develop arched tops. The roofs of those caves which rise still higher and reach or pass the present high water mark of the lake, lose also their wedge form and develop wide arches or even flat roofed tops. In the latter instances it is apparent that cave-widening agencies have become more effective than those bringing about upward ex- tension. A few caves have been developed upwards far enough to teach the cliff top. Among these are to be found a still smaller number that have had a portion of the roof fall in some distance back from the shore line. These therefore present us with small sink holes and natural bridges. Where these caves occur they de- velop in rather close proximity to each other, so one has to go but a few rods to pass many small mouths. The general external appearance of these caves where well de- veloped, may be seen in plate 1 —'a view of a portion of the north shore of Paradise bay on the east side of the island. The wedgelike form and close proximity of the caves are both well shown. The cave near the middle of this view has a sink hole some distance back and a natural bridge between it and the sea wall. A view of this small sink hole is shown in plate 2. The sea wall here faces south- east by south and is only subjected to strong wave action during 162 NEW YORK STATE MUSEUM southerly gales. A breaking wave rarely throws spray as high as the top of the cliff. Where the lake bottom, just off the foot of § the cliff, can be seen at low water, it is found to consist mainly — of bare bed rock. Pebbles as abrading tools can rarely be used against this wall and the water here never picks up enough sedi- — ment to become in the least discolored. 3 Plate 3 presents a view of a portion of a cliff about a mile distant ; from that shown in plate 1 and on the opposite or west side of the — island. Here the wall faces west by south. A few of the caves developed on easterly running joints have somewhat the appear- — ance of bedding or pebble-eroded caverns. It may easily be seen — that the influence of the bedding in their formation was slight, for the lower portion of the cliff does not differ enough from the upper — in character to make it a very effective factor. Neither can we ~ very seriously entertain the idea that they were pebble-cut, for the water near their mouths is now too deep to allow waves the use of a any visible abrading materials. Waves can break against these — cliffs only during westerly winds. The nearness of the mainland ~ prevents a very heavy sea and westerly winds in this region are of short duration. A little to the left of the region here shown the a cliff face turns easterly and there, on southerly running joints we : find the typical wedge-shaped forms like those shown in plate 1. A little to the left of the center of plate 3 is a cave opening that — reaches nearly to the top of the cliff, the cave here developing on a southerly running joint or fissure. This cave has maintained © much of its wedgelike character and the influence of neither weaker ~ bedding nor pebble-cutting is at all apparent in the outlines of its — mouth. In their earlier stages all of these caves were no doubt de- — veloped through the same agencies. A very large part of the present 4 difference between the caves shown in plate 1 and those shown in plate 3 may be due to the effects of glaciation acting on the fatter. We may note that southerly facing cliffs would be in a measure protected from strong glacial action while westerly facing cliffs would receive no protection from a planing action which would cut across their cave mouths. The form of the most distant large cavern on plate 3, the shape of the cliff face just south of it, and the — stranded boulder removed from this wall, all suggest glaciation as a modifying agent. Additional evidence to this effect will be pre- sented. Near the cliff shown in plate 1 is a small island called Spoon island which is separated from Valcour island by a narrow glaciated channel. A portion of its west wall as it appeared October 2, 1909, ydeisojoyd ev woly ZOOI UL Udye4 ‘UdIMIJIOG ISPIIq [eINJeU [[eUIS & YIM Yoeq VoULIsIp sUIOS [OY YUIS v Sey pue FID oY} JO advy oy} Ivou doy oy} je usdo SI a[pPpiut oy} Jeou oAvd oY], “YINos Aq }svayJNos Sule (puPISI noseA FO opis Jsva uo) Aeq asipeieg ul HYD I 93%Id Cee ~ = ey 2 aD TY / 4 ( Plate 2 View of a small sink hole some distance back from the cliff face shown in plate 1. There are indications here that this opening was due to the crushing in of the cave roof by the pressure of glacial ice. The small light spots in the lower left part of this opening are portions of the distant cave mouth. From a photograph taken November 2, 1909 uoyey ydeisojoyd ve wot ‘yanos Aq 4soM SodeF IIo JO 9YyT, ‘6061 ‘6 319qG0}90 I] 94} Jeol PURIST MOd[TeA JO APIs Jsom OY} UO PID & JO UOTJI0d & JO MITA “OsHoyyy g -O SC arprsy "JOYS I UISUOSSTAA OY} FO JUOTOAOW ay} SulInp AeMe Potiivd otaM suOoT1od JojnNo pue JapjoO ssOyM SsoAvo fo Spuo Jouul pue Josunod oy} ‘AyjUoredde ‘surejot YOIyM s9efIns pojeroeys Aypojqnopun ue sjuasoid d1oy YI sy, “6061 ‘2 JaqojIQ Usye} Yyder1sojoyd e Wo1f} pues UoOCdS fo ][[eM JsoM OY} Fo uolJod VV ” SIXTH REPORT OF THE DIRECTGR I90Q 163 lis)shown in plate 4: This wall still retains for the greater part lits former glaciated surface.. The whitish horizontal band, due to the dried remains of a sheet of green algae which covered this )portion of the wall in the spring, is an indication of the water level Jat that time. It may be noted that the portion of this wall covered /by water the greater part of the year is better preserved than either the portion only covered in spring or the portion above this which lis now never covered. The water surface shown in this plate cuts lacross the mouths of several small wedge-shaped caves or cavelets ‘and their appearance is very suggestive of glaciation after their formation. The clean and sharp junction with the smooth curved glaciated wall makes them appear like the younger ends or remnants of older and larger joint caves. The fact that a very marked and glaciated notch has been cut out from the under portion of the cliff just north of them and at their level, may be taken as indicating that a few closely packed joint caves had here so weakened the cliff as to allow glacial action to carry them in part away. Their former presence is shown by their bases which still exist. The well preserved character of this portion of the wall is due to the proximity of Valcour island on the west, to-a bar at the north (here indicated by the faint lines of surf), and to the fact that waves from the south are broken by cliffs as they enter the channel. There are a few instances in which these caves have followed bedding planes, and cut such wide and deeply penetrating caverns as to bring down great masses of the rock above. Plate to repre- sents a portion of the shore of Valcour island as seen from the south end of Spoon island October 23, 1909. The great fall of Tock at the left end of the cliff is due to the collapse of such a cavern. A little to the right of the middle of this view there arises from under the water a second low but wide cavern which follows the bedding plane seen at the right. The vertical dimensions of this cavern become rapidly less as we move up along the bedding plane and they become practically zero before we reach the highest part of the dried algae belt, plainly seen as a whitish band parallel With the water surface. The width is considerably greater than here shown because it extends to the left under water. The distance to which it penetrates the cliff horizontally was greater than could be determined: The wall here is a north and south fault scarp, is on the upthrow side and is but a few meters from the fault line itself. Not far back of this we find a few parallel faults with very small vertical displacement, but revealing, by slickensided. surfaces, a larger horizontal component. The cliff to the right of the portion 1604 NEW YORK STATE MUSEUM here shown presents some nearly horizontal joints which curve up southerly and cross the beds. The block here has been subjected both to a strong uplift and to a thrust toward the south. The in- dications of vertical and lateral displacement make it quite possible that these aberrant caverns are also following some preexisting planes of fracture, and that they are in their origin not essentially different from the caves first mentioned. The other cave mouths which show on this plate illustrate clearly the tendency to acquire verticality. Now numerous as these joint caves are, they are found with a single exception where the present water line of Lake Champlain either just keeps them covered or cuts across their mouths during some portion of each year. The high water level of spring leaves but comparatively few of them uncovered, but the number brought into view rapidly increases with the lowering of the water level. In other words, the floors of all but a very small number of these caves lie a meter or more below the present low water level of the lake while their roofs stand at varying hights above this level, some of them reaching far above that of present spring floods. Their horizontal depth is not so easily measured but many small mouths give forth deep bass notes when any sea is running and their boom- ing may be heard for considerable distances. A few can be fol- lowed into the cliff for several meters but a narrower portion may be always seen to penetrate to still greater depths. Plate 5 shows a sink hole many meters from the shore line and the sink hole shown in plate 6 is 150 meters from the nearest lake margin.* =< *The sink holes shown in plates 5 and 6 both seem to be of com- paratively recent origin. In plate 5 a border of fresh earth, on which nothing was growing, is to be seen around the front of this opening. This feature and the overhanging sod at the left are indications of the removal of much earth in a single season. If anything like an equal amount has been washed out each season the sink hole can not be many years old. That it was covered in comparatively recent times is also shown by the presence of portions of old stumps and roots on the rock surface of the more distant border of the pit. It does not seem likely that we are here dealing with a recently fallen rock roof but it does seem likely that such a roof was crushed in during the last stages of the ice sheet and that the opening was then filled with till and after- ward covered by Pleistocene deposits. As soon as the present land had lowered sufficiently to allow waves to run in and out of the cluster of narrow caves here seen to connect this pit with the lake, the water would undermine and carry away these deposits and so allow the sur- face to finally cave in. Such a conclusion would make the caves con- necting this pit with the lake, preglacial. 6061 ‘QI 19q0}9Q uoye} ydeisojoyd eve WoT “Yous oy} Fo spus oY} SuUIyxIvUF SMOLIL ol} ‘A][BOJAOA YS Jojour Ve dn sulpjoy st vs[oy oY} Ul Wosied ayy, ‘Hoop IwoqtueoIs Plo oy) JO YINos souEISTp JsoyS eB “PULIS? AMOOTB/ FO SPs) souk oY) WoO spo qurs Be yo Mer Plate 6 zs mite Sink hole on the lower terrace (meadow) of the north farm and 150 meters from the west shore of Valcour island. From a photograph looking north by west and taken October 10, 1909 ra Plate 7 Block of pure dolomitic limestone, of Lowville? age, cut by confluent cupholes. Vertical distance from table surface to upper point of block 463 millimeters. Specimen now in the New York State Museum Plate 8 View of fractured end of the lower portion of the block shown in plate 7. Presents a side view of the cupholes and forms of figures produced by nearly vertical sections of the same. Shows also the edge of the dent- pitted surface below, and indicates approximately the comparative value of the two forms of erosion as geological agents SIXTH REPORT OF THE DIRECTOR 1909 165 The very marked relation of these caves to the present water levels of Lake Champlain strongly suggests this lake as their cause. On the other hand, the vertical’ depth to which they descend below low water, their increasing number at the lower levels, their great width and horizontal depth, their appearance on fresh glaciated sur- faces and their apparent modification by glacial action, all strongly suggest a preglacial origin for them and leave them as rock 1n- scriptions commemorative of lake Valcour.* During the past season these caves have been studied with the hope of finding evidence which shall serve in determining their age and the manner of their origin. It is the purpose of this paper to present the evidence found. The first of this evidence deals with a peculiar feature of erosion found on all cave surfaces which have been acted upon by the present lake waters. It will be necessary to treat this feature somewhat in detail and this we propose to do under the subtitle which follows. Dentpits. The beds of the uppermost Chazy are in part cov- ered where they crop out at the northeast corner of the island, but under the water of the lake and some distance out from the shore line, wave action has swept them comparatively clean. During the period of phenomenally low water in 1908 a series of samples of these beds, which run from just below the sandstone capping of the Chazy to the beds of the Black River epoch, were secured. One bed of very pure dolomitic limestone of Lowville age (?) was deeply cut on its upper surface by confluent cupholes* whose edges were so sharp that it was an exceedingly painful matter to stand on them barefooted even though the water was more than a meter deep. This bed had been undercut, and a large block had fallen from its edge and now lay in a number of smaller pieces. These pieces however still remained in their proper relations to the bed and to each other and none of them had been turned over by wave action. On raising a piece of this bed weighing a little over 46 ' The sink hole shown in plate 6 is in a meadow on the lower terrace of the north farm and seems to be a still more recent opening. This hole had been partially filled up with some old cedar stumps, and three upright poles served to indicate its position to any one mowing the field. These stumps and one of the poles were temporarily removed in order to obtain a view of the rock edges in the opening. This opening Was not sufficiently illuminated to allow its interior to show any detail in the photograph. . *See Some Items Concerning a New and an Old Coast Line of Lake Champlain. N. Y. State Mus. Bul. 133, p. 159-63. “loc. cit. p. 160-61, pl. 1-5 inc. 166 NEW YORK STATE MUSEUM pounds, my attention was called to the very peculiar and clearly cut: pattern on its under surface. As this block must be considered in evidence, it is represented here on plate 7 to show its upper surface, plate 8 to show a section through upper and under surfaces, and plate 9 to show the under surface. During the early summer of 1909 an examination was made of the cave whose arched mouth, rising just above the whitish dried algae band, may be seen a little to the left of the center of plate 10.. Here a peculiar erosion pattern similar to that on the under side of the limestone block referred to [pl. 9] was discovered but with this difference: on the limestone block the surface was of small area and all the dentlike depressions were confluent ; here the pattern was spread over many square meters of surface and varied in its degree of complexity all the way from the separate circular depressions near the mouth of the cave to the horizontally alined and crowded pattern of the deeper recesses. Plate 11 is from a photograph of a portion of the north wall of ~ this cave taken August 1909. The depressions are least crowded in the upper right-hand portion of the plate or in that portion of the cave nearest the mouth and under water action for the lesser portion of each year. A distinct horizontal arrangement of these depres- sions is to be noted, and we are compelled to attribute it to the direction of the flow of water in and out of the cave during wave action, and not to bedding planes. For convenience in reference we shall call this cave Bat cave. On visiting the recesses of the cavern with a fallen roof, near the left end of the cliff shown in plate 10, a still more remarkable arrangement of these depressions was discovered. Plate 12 is from a photograph taken October 2, 1909. We are here looking westerly across a higher portion of the inclined cave floor, and the lines taken ‘by the confluent depressions are clearly seen to take the natural lines of water discharge. Even in the vertical fissure shown ° here the lines are not horizontal and neither would be the direc of the outpouring water as a wave receded. Plate 13 is a view which penetrates deeper into the cavern than did. plate 12.. The vertical fissure at the left of plate 12 is seen at the extreme right of plate 13. In this last plate the relation of these lines of confluent depressions to the direction of water flow 1s still more striking. An examination of these two plates will also reveal the fact that the sharpest lines of intersections lie deepest within the cave recesses where they are protected from other a eee <<“ we reXs en ven oe é = ="

of that which is allowed or used in the cutting of cupholes, Keeping in mind the statements just made, let us examine the shores of Valcour island. Where cupholes have not become confluent they are cut on distinctly glaciated surfaces and their SIXTH REPORT OF THE DIRECICR IgO9 ee depth rarely exceeds 10 centimeters. Where dentpits have not become confluent they may also be found on glaciated surfaces and the markedly slower process of their formation has rarely allowed them to penetrate to a depth greater than 1 centimeter. Scattered dentpits on an undoubtedly glacial surface may be seen in plate 4, on the smoother surface of the rock and about half way between low and high water. Foreshortening makes them appear as ellipses. A little above this belt and near the extreme right a few more nearly circular outlines may be detected. These dentpits are of precisely the age of the cupholes and both were started on glacial surfaces when the water was lowered to near the present level. Now, just inside of the mouth of Bat cave in the opposite wall of the channel and at the same level, we may also find a few separate dentpits but much better developed than those on the wall outside. Where cup- holes have become confluent they have of course destroyed the glaciated surface. In these regions of greater activity the surface may have been cut away to an average depth of perhaps 20 centi- meters. Likewise with dentpits, where confluent, the vortexes pro- ducing them were the more numerous and stronger and the amount of surface removed may have been as great as 2 centimeters. This is the condition of the cave wall shown in plate 11. Now as this cave is more than a meter wide it follows that im all tts essential features it 1s as old as the glaciated surfaces on which the: dentpits are cut outside. ‘The recognition of these dentpits and a knowledge of their rate of formation thus enables us to decide a very important question and the answer is evidence of the strongest character for preglacial or interglacial Lake Valcour. 3 As dentpits stand in such an intimate relation to solution it will be important to consider next this factor in the formation of the Valcour island caves. Solvent power of Lake Champlain on its limestones. Cystid point, on the southeast shore of Valcour island, seems to be caused by the presence of a fissure, and the little cove just south of it is filled with movable rock debris to a depth of about 2 meters. On either side of this cove the shores consist of bare rock. Suspecting the eastward extension of a fault here, I have made an examination of the visible lake bottom from a rowboat on a perfectly still day at a time of low water in the fall of the year. The condition under water was much like that noted on the exposed shore. A depressed belt over the fissure was covered with boulders and pebbles of various kinds and sizes while, on either side of this, large areas of 174 NEW YORK STATE MUSEUM bed rock were free from loose material. At some distance from the shore the material covering the belt was such as we should expect to find in a region of washed till. The belt was here neither — so wide nor so thickly covered as it was on the exposed shore. Wave action had evidently assorted and built up the shore de- posit but the deposit under deeper water seemed to have suffered little if any movement. Under about a meter and a half of water we noticed a pebble about the size of a cobblestone which was resting with its bedding planes in vertical positions and which appeared to show the results of differential solution in a rather interesting manner. The ar- rangement of its alternating layers of very fine silicious and cal- careous sediments seemed strikingly like that of a peculiar bed found on the island only in the weakest part of the Camarotoechia shales. Its calcareous layers had been dissolved or eroded to con- siderable depths, leaving the projecting silicious layers as an index of the former size and shape of the pebble. One aspect of this specimen is shown in plate I5. When broken from its bed, during the last glacial period, or when separated from the larger block of which it may have formed a part, it evidently had the form of a four-sided prism with faces of unequal area. In our figure it is resting on the remaining portions of the largest of these former faces, which is much foreshortened in the view, and it has what is now left of its former smallest face, at the lower front. The latter face has-been wholly lost from the softer portions of the stone and these now possess an acute angle in place of it. This prismatic form was considerably modified, during its movement with the till, but was not wholly lost. Glacia- tion seems also to have added a few facets. Any marked wave or water action on this specimen must have been absent during the existence of Lake Vermont and the Hochel- agan sea, for those were times of deposit in this locality. When Lake Champlain began work at nearly its present level it had first to remove these later deposits and wash out the finer material of the till before it could begin to work on what then must have been a smooth glaciated pebble. The cutting out or the dissolving of the softer portions of this stone must therefore be purely the work of Lake Champlain and of no older body of water. Its study should yield testimony of great value as to the ability of this lake to have formed the series of caves which now lie along its Valcour island shores. Piatesns MN OE 6 BS) , 43 * 4114 One aspect of a glacial pebble which has lost much of its substance through differential solution and erosion by Lake Champlain SIXTH REPORT OF THE DIRECTQR IQOQ 175 We may first note the exceeding thinness of some of the re- tained silicious laminae which now project in places as far as three or more centimeters beyond the surfaces of its cal- careous layers. The edges of some of these sheetlike exten- sions are so fragile that they were broken in several places dur- ing the careful handling which the specimen received before being photographed. The edge of one recent break may be seen in the middle thin sheet of plate 15 and is shown in plate 16, figure 2. That these and other fragile edges had been pre- served shows conclusively not only that the specimen had not been rolled by wave action for ages but also that wave action had not been able to roll or throw smaller pebbles against these edges since they were formed. This witness against the power of wave motion in this locality to use small pebbles as tools of erosion would lead to the conclusion that this speci- men, when found, was resting on the same base on which it rested at the time of cessation of motion of the last ice sheet. This may be true, but there are two different times in which this pebble may-have been moved and it will be well to note them. The bare areas mentioned may have been first cleaned off by sub- glacial drainage moving under pressure and the pebble may then have been removed from the till to find permanent lodgment in the more sheltered position over the fissure. If not moved before the ice front passed to the north it could not have been moved until the waters of Lake Champlain had arrived at ap- proximately their present level. While Cystid point is some- what sheltered from storm action yet it is no easy matter to land here in a rowboat during strong north or south winds. Waves of exceptional force may have swept the till from the bare areas mentioned and moved the pebble to the deeper and better protected position in which it was found. Whether left in this position by the ice sheet or moved thither during either of the periods mentioned above, it could have been subjected to solution or abrasion only since the deposits of the Hoche- lagan sea were swept away. If for long ages wave motion had been unable to use small pebbles against its thin edges it must have been unable even once to turn this specimen over during that same long period and the erosive features we are about to notice will yield strong evidence in support of this conclusion. One face of the supposedly dissolved portions of this specimen is unmistakably marked by typical and confluent dentpits with 170 NEW YORK STATE MUSEUM widths of about 10 millimeters and depths of from 1 to 2 milli- meters. The presence of dentpits shows us at once that these softer layers have not been cut away by simple solution but that erosion at the hands of vortex motion has played an im- portant part in the process. Remembering also that dentpits show absence of cutting vortex points loaded with sediment by gravity, we find them in this case indicative of surfaces which can not well have been upper surfaces. The two sur- faces on which these dentpits appear are both on the under- side of the specimen as it is shown in plate 15, or on the broad- est face of the present three-sided interior prism and are only separated from each other by the thin silictous sheet of the middle bedding planes. As in this plate the specimen is rest- ing on the remnants of its older prismatic face of greatest area, which was the position in which its center of mass would be lowest, it would appear that these surfaces were not only under- surfaces when found but that they had been such during the whole age of Lake Champlain. These two dentpitted surfaces of the softer beds of the stone have been cut by abrasion and solu- tion together until they are now 27 millimeters distant from the outer edge of the harder layers or from the probable surface of the stone as the last ice sheet left it. This aspect of the speci- men is shown in plate 16, figure I. The surfaces of the soft beds which are opposite the sur- faces just described are indented with numerous, more conical pits, measuring from 2 to 3 millimeters in diameter and having about half that depth. The cutting here is of the type effected by vortexes whose points are down, and kept filled with sediment by gravity. Though the dimensions of these cuts are so small, they have lowered this surface of the specimen some 55 milli- meters. As cutting of this type can take place only in a down- ward direction the surfaces of the specimen on which they ap- pear must have been upper surfaces. ‘These are the surfaces uppermost in plate 15 and the greater rapidity of the cutting on this portion of the specimen only served to lower its center of mass the more and make its equilibrium still more stable. These surfaces have very probably been upper surfaces ever since the cessation of motion of the last ice sheet. This as- pect of the specimen is shown in plate 16, figure 2. The character of the two soft layers does not change on pass- ing from one side of this stone to the other and the difference UMasnyy 2381S YIOK MON ot} UE Mou uostTIedS ‘SOdIJIOA JoyeM FO sjutod papeo] jnq [Jews Ay;sutposoxo AueUI Aq JN Used ALY 0} ooefins toddn oy} smoys 2 Ins ‘sid JUap JUsNyUOD pue [eordAy Ysnoy} [jews Ave] 0} SB JOUURUT B YONS UI soxa}IOA JoyeM Aq JND Ussq IALY O} Speq jFOS 94} FO soVjins Jopun oy} sMOYS I JING ‘mejdmeyy oye] FO JoyeM Jsamoy MOTOq Yidap Stojou eV ISAO 9I}}I]T B WOIF Uoye} atqqod popoOte-loyeM PB JO SMITA OMT, ne in oe OOo ae fo Cue ) ye). : Wave iy wo J i ae : 5 : / J 1A ; sie caitlin ett dt ,olt, |e . fe ley | Tot elt pelt) te Or, je) je, jay id alr a) Bs t 9) Jou Jey. CT LL LAE TTT TT TTT TTT eT mm p : l gI aie Id SIXTH REPORT OF THE DIRECTCR IQOQ 18 FF in the depth of the cutting is due purely to a difference in the action of the environmental forces. When this specimen was first taken from its resting place no attention was given to its position on the bottom other than that its bedding planes were vertical. In other words it was not noted which side was upper- most. The two distinct types of erosive action we have been discussing have, however, enabled us to very positively determine this matter some years after the date of collection. Not only have they done this but they also have strengthened the con- clusion, drawn from the thin edged laminae, that this stone had never been moved by the action of heavy seas but had remained with its dentpitted surface down for several thousand years. It may here be noted that this pebble yields information of Mermeanmotaer variety. ‘[hat the floors of many of our.caves are a meter or more below the present lowest water level of the lake would in itself be evidence that this lake did not cut them unless it had for a long time been at a lower level than the average of the last hundred years. Now it could not have been that meter lower without having brought the specimen we have | been discussing so near to the surface that the waves of storms would have used it as a plaything, deprived it of its thin edges, destroyed the remaining evidences of its former angular out- lines and made of it a simple beach pebble. Its fellows would also have been so changed in position as to bear witness of the segregating power of wave action. Our pebble thus yields evi- dence that goes to prove that the surface of Lake Champlain has never been materially lower than it was in November 1908, and never before perhaps so low. The old benchmark in Shelbourne harbor made in 1827 marks the exceptionally low water reached that year. Not till 1881 was this mark passed and a new record established. In No- vember 1908 this was again passed by about 2 inches. As the pebble we have discussed is in itself testimony that the lake has never been lower since the period of the Hochelagan sea and as it bears on its surface an index of the work accomplished only ‘since the present lake waters were low enough to uncover this pebble, it becomes in itself a timepiece showing the age of Lake Champlain. In other words this pebble presents clear evi- dence which goes to show that on the melting of the ice sheet, iso- static balance was quickly restored in this region and a position close to a former water level, that of Lake Valcour, was rapidly recov- ered and has since been held. 178 NEW YORK STATE MUSEUM Let us now take the evidence this pebble has to offer con- cerning the question of cave formation. As it has rested at a level close to that of the floors of many of these caves for just as long a time as Lake Champlain has been in existence, it should be able to offer a fair measure of this lake’s capacity to dissolve its limestones and to erode them through dentpit formation. At Cystid point these two agencies have cut com— paratively pure limestones to the depth of but 27 millimeters. It does not seem likely that the deeper purer waters of Para- dise bay could, in a more sheltered position, have cut to greater depths during the same period. Many of the caves of this region, however, represent a cutting more than 75 times as wide and several hundred times as deep. Portions of their walls are out of water for more than half of each year and are then free from any action of this nature, but the pebble has remained under water for every. moment of every year. The results =enims comparison are very striking and perhaps are not wholly fair. It may be urged that vortex action would be stronger and there- fore more effective in shallower waters. This may be true, but the greater depths of the caves have also been subjected to this action for every moment of every year and under this depth we shall probably be again dealing with vortexes whose strength is no greater than those of the pebbles’ level at Cystid point. Most of the cave walls maintain their wedgelike shape and be- come wider as the limit of low water is reached. Weighing carefully the evidence, we shall make ample allowance for the results of these two features of wall cutting if we credit them with the removal of between 2 and 4 centimeters of surface during the age of the present lake. The evidence of the pebble is therefore to the effect that Lake Champlain has been at most but a modifier of a belt of old caves which were very evidently left here by an ancestral body of water. Valuable as has been the evidence this specimen has given us, it has yet failed to show that for which it was taken from its position of long rest. In other words it has failed to clearly show the amount of solution accomplished by the present lake. We have merely found a very definite limit which solution could not have reached in the time involved. It should be allowable however, and helpful as well, to make an approximate or tentative estimate of the share each agent has accomplished in this recorded work. As a whole, abrasion is a much more powerful agent than SIXTH REPORT OF THE DIRECTOR 1909 179 solution, but we are on very uncertain ground when the abrasive material used is as fine as it must be in this case; and also when its particles are so much freed from the influence of gravity. The practical absence of evidence for differential solution on dentpit surfaces, however, is a very good indication that molar abrasion is here still the most important factor. We may allow it at least two thirds of the 27 millimeters noted. The remaining g milli- meters will then become an index of an utmost limit for the amount of erosion accomplished by molecular abrasion, solution in presence of a rapidly moving solvent, and solution in a quiet solvent or where molecules and ions can escape from the contact films only by diffusion or movement induced by gravity. As the rapidly deepening rill channels on roche moutonnée slopes are by themselves strong evidence of the powerful influence of a rapidly moving solvent, and as our previous discussion shows that we should expect it to be such in both this type and in dentpit formation, we may assume that vortex motion through molecular abrasion, through bringing the greatest volume of water in contact with a given surface in a given time, through forceful detachment of portions of saturated contact films and through various trans- formations of energy, is responsible for at least two thirds of this g millimeters, and that quiet normal solution, relying on simple gravity or diffusion to further liberate the molecules which have passed into the contact film of the solvent, is responsible for not more than 3 millimeters of a surface on which it has been acting for 50 centuries or more, which is the time we may temporarily assign for the age of Lake Champlain. While, therefore, solution may have played a very important part in the formation of these caves, it was very certainly not solution by the waters of our present Lake Champlain. Additional evidence as to the effects of solution is to be found in Sloop bay. At the foot of a cliff which terminates the horizontal depth of the bay there is exposed a wide glaciated shelf which dips gradually southerly and enters the present waters of the lake. The higher portions of this shelf are still covered by till and show the usual scratched and polished surface of the rock, when un- covered. That portion which has longest been uncovered, save at highest water of spring floods, has been acted upon by expansion of water freezing in its joints and bedding planes, and large blocks have been loosened to be pushed about by shore ice or dragged sea- ward by ice blocks during the breaking up of the lake in the spring. 180 NEW YORK STATE MUSEUM As the shelf approaches low water it reaches a level where the action just described is inoperative, and the surface sheet of rock has not been removed. This surface sheet is swept clean of sediment and is much as the ice sheet left it. The bed here had its constituent sediments assorted by vibration of the bottom waters of the Chazy sea, due probably in part to wave motion on the surface and in part to tidal flow of waters over the surface of the sediments. A series of interlocking ridges containing much silicious material were thus segregated and the bottoms of the miniature valleys between filled with the finer and purer calcareous material of the bottom. Solu- tion aided by mechanical attrition has carried away the exposed softer portions of this bed to a depth frequently measuring 24 milli- meters and sometimes slightly exceeding this depth. A view of this shelf at a time of low water is shown in plate 17. The ridges remain as flat surfaces of irregular outline. Abrasion has removed the glacial polish and finer striae from these surfaces and there is a slight relief of a fraction of a millimeter in some places which reveals figures like branching algae with stems from 2 to 6 milli- meters in diameter. The amount removed from the higher surface can not well be more than I or possibly 2 millimeters, the aver- age loss of surface from the softer and harder portions being in the vicinity of 15 millimeters. The bay opens to the east and there are no strong winds from this direction in this region. North or south storms disturb the waters here but very little. The bay however has a muddy bottom and storm action enables its waters to take up enough sediment to become discolored. At such times small and gently moving waves with an abundance of fine abrasive material must lap this area. Careful examination of the lowered surfaces of the rock plainly show the presence of water vortexes carrying silt. The difference between the 55 millimeters of the block last studied and the 24 millimeters of surface removed here must be largely due to the great difference of wave energy in the two localities. Whatever part has been played by solution in the lowering of the Sloop bay surface has been aided in no little measure by plant action for blocks taken from this surface show a dried organic film still attached to the very irregularly pitted sur- faces of the depressions. The depth of 24 millimeters is not to be found next the harder ridges but near the middle of the softer area. Solution alone would have worked with greater uniformity. As in even the lesser depths, erosion by vortex action is still a factor, it hardly seems possible that pure solution could have “QORJINS poyeloep[s IJ9W4O} 94} MOTEq StoJouMTjJUeD € pue © UsIMjJoq JO OUL}SIP & O} JOYS sty} Fo suorijsod J9}Zos oY} JNO oAeY “UOTSeIge [BOTUeY OU Aq popre ‘urejduiey) oye] FO siomod JUSATOS IY], ‘9061 ‘6z Joquisjdag uo Jo}eM MOT SulmMp usyey “Arq doojS ur Jjoys yoor e fo ydeirsojoyd ev wor Lt 93e1q SOx "REPORT OF THE DIRECTCR I9Q0Q ISI removed more than a very few millimeters of this surface. Now the periods of time involved in the cutting of the dentpits, the softer layers of the pebble from Cystid point, and the softer layers of the rock shelf here are practically equal, for the phenomena occur along the same horizon. When once the waters of Lake Champlain had reached their present level it would not take shov- ing blocks of ice very long to clean off the Sloop bay shores and leave them very much as we now find them. The amount of rock surface removed by the solvent action of the incessantly changing, and far from saturated, waters of Lake Champlain is shown by these studies to have been remarkably small. A still more conclusive bit of evidence concerning solution is to be found along the more southern portion of the west shore of the island. There is a line of low cliffs along a considerable portion of this shore, and it often rises several meters above low water. These surfaces are exposed to wave action from seas raised by westerly winds. Such waves here carry little sediment owing to the deep water and clean rock bottom just off shore. That these waters are deep is indicated by the presence of the ruins of an old dock here at which the largest lake steamers used to stop to take on wood in the days when that was the available fuel. A view of this region is shown in plate 18. The long oval rock basin of the fore- ground, considerably foreshortened 1n our view, is but one of a number of such basins cut by the till on the old shore line of Lake Valcour. The debris seen in the basin has been derived from higher portions of the shore line through the effects of freezing water in joints and bedding planes, and the action of shore ice. The amount of the destructive work of Lake Champlain on this older glaciated shore line may be easily seen. The principal, and by far the greatest cause of loss, has been due to the effects of freezing water in joints and bedding planes and the subsequent removal of the loosened blocks through the action of shore ice. The ma- terial now lodged in the glaciated basin is a portion of the material which was so derived from the surface above. Wave action itself, even with the load of tools here present, has been rather an unim- portant agent and has not been able to modify appreciably the basin in question. A nearly complete portion of an old glaciated outline of this ancient coast may be seen where the figure is present. One block has been removed from the surface on which she is standing but much of the old glaciated surface remains above and to the right of her head. The shelf on which the boat rests has been 182 NEW YORK STATE MUSEUM somewhat cut by cupholes. The edge of a still older, upper ter- race, which Lake Valcour was destroying, may be seen directly above the head of the figure. The old steamboat dock is hidden in the second cove beyond the boat. In plate 19 we have a view in this region taken farther to the north and near the position of the old steamboat dock. Another glacial basin, partly filled with rock debris, is here shown. The rock boss at the right of it has not yet lost its glaciated outlines although freezing water has de- tached one block from its surface and the movement of shore ice has drawn it a little outward. We have here a practically unbroken glaciated outline reaching from low to high water. While the lake was yet above its present level the side of this boss facing the lake must have lost the sediments with which it may have been covered. Its surface has been exposed to the action of solution throughout the age of Lake Champlain. While the movement of loose material on this surface has destroyed glacial striae yet such striae may be seen on surfaces at the same level just south of this. There are places here that have not lost 5 millimeters from their former polished surfaces and we are obliged to limit the solvent power of the lake waters to a figure at least as low as our estimate made from the study of the pebble taken from Cystid point. If one is still in doubt as to the correctness of this estimate let him exam- ine again the west side of Spoon island as shown in plate 4. The unbroken glaciated surface shown there runs from below lowest water to above highest water After allowing for loss of surface at the hands of various agents active here, what will you have left for simple solution? The well developed caves of plates 1 and Io lie between 60 and 180 meters from this face and on the same level. What part has solution, at the hands of Lake Champlain, played in their formation? Before leaving this question of solution we should call more definite attention to an agent we have but mentioned, and that is the influence of living or decaying green algae, sponges and micro-organisms. If we again examine plate 9 we may note that this surface of the Lowville block has a border of dentpits which distinctly show the effects of differential solution brought about by the above cause after the block had fallen from its bed. Nearer the center of the block there was not light enough to sup- port plant life and the dentpits of this region have suffered but little change though there are a few thin seams of less solvent material running through the block that have here formed very Qo61 jshsny Ul Usxe} ydeisojoyd Be Wor poqeper[s oy} Jo 9ut0s Surmoys ‘puvyst inoseA FO QI aieIq ‘InNos[vA We] FO o10ys a10ys ysemyynos oy} FO uonsod e@ JO MaIA V ‘MIOp Jeoquivsjs pjO ‘psAo1sop oAvrM oy} FO ied & SI UIseq pojelorps 94} puosoq jsnf jurod oy y “JoyVM YSty 0} MOT WOIF oUTTNO JeIDe[s usayorqun ATpeoOe.1d ev smoyS “6061 ‘OI JaqojIQ Usaye} Ydersojoyd e WoO pULIsI INOIeA JO o10YS JsamyjNos oy} FO uoTZIOd & Jo Moar ar os 61 93e[q a e eae a, ‘4 , — = y) — i = ‘ ~ SIXTH REPORT OF THE DIRECTOR IQOQ 183 fine and slightly raised lines which follow the rise and fall of the dentpit surfaces. Such elevations on the general relief of this surface are in no case greater than a fraction of a millimeter. This type of solution is due to organic acids produced by resi- dent organic forms, and is chemical in its nature. The cave walls are protected from this agent, save in an indirect way, for they are shielded from light. The lake waters themselves of course hold carbon dioxid in solution and the supply is constant and from various sources. It has no doubt markedly increased the solvent power of Lake Champlain waters but its effects lie within the limit of the 3 millimeters already set as the greatest limit of quiet solution since the recession of the Hochelagan sea. Effect of expansion of freezing water. We have already called attention to this most powerful of all the disintegrative agents now at work on Valcour island in our remarks covering the features presented by plates 18 and 19. ‘The vertical or overhanging front of the cliff shown in plate 1 is very largely due to this cause. In the Fourth Report of the Director of the Science Division [N. Y. State Mus. Bul. 121] plates 5 and 6, will be found two reproductions of this cliff from photographs which I made in the winter of 1903. Both views were taken from the ice surface shown in the foreground, and both contain a view of some portion of the cliff shown in our present plate 1. The ice curtains, which speak of frozen spray, have a very interesting story to tell of cliff destruction. The effect of this agent is here seen to be destroying caves instead of making them. The most numerous and most marked changes in temperature occur on the exposed faces of these walls. The waves break here and wet the surfaces to great hights. The lake waters themselves are rarely frozen over (save for a few days) until some time in Janu- ary. The fall rains raise the level of the lake and many small cave mouths are covered in consequence. The water in these is mever frozen. It is doubtful if the water in the innermost recesses of some of the large caves is ever frozen. Once well within one of the higher caves and we shall find wetting above the water line to be but a fraction of the hight to which it is wet outside. The dentpit etching on the inner wall faces speaks of their comparative permanence, as do also the rounded edges of the rock angles. On the outer face of these cliffs, where blocks have been split by freezing water, no surfaces are etched and all rock corners are sharp. At the south end of the island 184 NEW YORK STATE MUSEUM where most of the Chazy beds are exposed there are but a few beginnings or remnants of caves in the very beds in which they should abound. ‘The cutting back of the cliff by the process in- dicated gives the cave-forming forces but little chance to outrun it. On the shore represented in plate 1 the wave energy is much less powerful owing to the projecting capes to the south. Here outer destruction follows inner formation at a respectful distance. At long intervals a fragment of the side wall of the caverns some distance in may become dislodged and plate 11 shows several edges that could be easily removed. A few such have been found in the debris partly filling some of these caves. How- ever large a part this destructive agent may have played with outside walls as we enter the caves its power is reduced with the distance to which we penetrate until finally it is entirely inoperative. It is widening the mouths of the caves somewhat - and increasing their hight in some instances but it is doing nothing to carry them deeper into the cliff. Evidence from preliminary excavation. The floor of Bat cave is deeply covered with blocks which must have fallen in greater part from the roof though doubtless there have been also many contributions from the side walls. An effort was made during low water of the present season to penetrate this’ “mass and find the cave floor. The first blocks removed were very heavy and showed little trace of either solution or erosion. Some of the unmoved blocks of this layer may be seen at the lower left in plate 11. The material we removed was all! carried toward the front of the cave and much of it thrown completely out. After getting down about a third of a meter the surfaces of the blocks began to show plainly the effects of differential solution, and at about a half meter this aspect became pronounced. For the next half meter the blocks had to be removed from under. water and not a single block was found that showed the least . sign of any movement in the mass. As a rule the lower blocks were smaller, but all possessed angular outlines and not one showed a rubbed surface. Some of these lowest blocks had edges so thin as to be easily broken off by the fingers, and all showed differential solution to a very marked degree. One Specimen taken from the depth of about a meter was photo- eraphed, and a view of it is presented on plate 20. A study of the surface and edges here shown will convince any one that wave motion since the glacial period can have had no effect Plate 20 From a photograph of a sample stone taken from about a meter below the surface of the material now on the floor of Bat cave. It shows conclusively that no one of these blocks is moved over the surface of another and that the cave is therefore not eroded through any shifting of this material. Specimen in possession of New York State Museum ~ SIXTH REPORT OF THE DIRECTOR 1909 185 whatever in moving the mass of material now in the cave. If other evidence were needed we could point out the fact that the dentpits extended down by the side of this debris as far as we made our excavations, and that the raised and sharp edges of intersection of the confluent dentpits were in no manner cut ies Or worn by any movement of the cave filling, Plate 11 shows a considerable portion of this uncovered face of the wall. The horizontal line a~—a separates the formerly exposed surface from that which we uncovered. The position of the camera was about a half meter above the surface of the filling and this will account for the apparent inclination of the lower lines of dent- pits. Not only had no marks been made on this wall by block motion but the wall itself had been cut away from the filling SeeeeetOesepatare one from the other. We hoped to penetrate deep enough to see if this loose material rested on any undoubted glacial deposit but the limit of time available led us to cease fur- ther prosecution of this work for the season. The material taken from the cave filling has itself some valuable evidence to offer. We have already seen that Lake Champlain has had but little effect on its rocky shores so far as pure solution Seeemrerica. Ehe material in this cave filling, at the depth from which the specimen illustrated by plate 20 was taken, shows a very marked amount of solution. An examination of this figure will reveal no trace of vortex action as an assistant factor in the cutting but it does show that the rate of removal depended entirely on the minutest differences in character of the bed material. Apparently no better example of pure differential solution could be desired. If there has been no help from me- chanical abrasion, the filling at this depth is most certainly older than Lake Champlain. The absence of movement in the mass on this cave fioor and the depth to which solution has acted on the deeper portions of the filling can lead to no other con- clusion than that these rock fragments were in the position in which we now find them before Lake Champlain began to cut its present series of cupholes and dentpits. The westernmost cave of the north wall of Paradise bay was next examined. Plate 21 gives its appearance as seen from the water edge at low water October 23, 1909. This cave is formed on a minor fault plane and close to it, both to the east and west, are parallel faults of small displacement. Freshly fallen blocks from the face of the cliff at (a) reveal nearly horizontal slicken- 186 NEW YORK STATE MUSEUM sides. That there was some horizontal movement together with a slight vertical displacement is also shown by the neighbor- ing faults. The cliff beds are much more fractured here than they are in the region immediately east, which is that shown in plate 1. Asa result the cliff face has here receded to the north more rapidly and has left the less fractured face some meters behind. The latter plunges vertically into the water but the more rapidly receding portion has left in front of it a sloping beach which crosses the cave mouth at the cliff line. This re- cession and the position of the cave, which is well within the bay, both protect it somewhat from the effects of freezing spray though we still have the active work of freezing of water after cold rains in fall and spring and the freezing of water from melting snows. During storms the strong elbow of the cliff protects the recess from the grinding effects of strong wave action, and the fragments on the floor are but little rounded. Probably the fragments now on this shelf are comparatively new, for oblique wave motion would carry the more worn ma- terial into the recess at the northwest corner of the bay. Here we do find a mass of material that is all of limestone and has accumu- lated in this locality since glacial time. The writer first saw this cave in 1898. The following year he camped in its vicinity and con- verted it into a very serviceable dark room for photographic pur- poses. One large and well worn stone lay partially within the mouth and this was removed to make the interior easier of access. One had still to enter on hands and knees, though after penetrating to the horizontal depth of about 2 meters, one entered a rather roomy chamber in which several people could stand at the same time. The roof of this chamber is about 3 meters above the floor. Back of this first chamber there is another but the pas- - sage between the two is too narrow to allow of entrance. A few blocks were carried into the first chamber to support a board which was used as a dark room table. The waves of the follow- ing season moved several large blocks against the opening of the cave but did not disturb the stones placed on the floor of the chamber. For several years blocks have been thrown up in the front of the mouth during spring storms and often one or more has had to be moved in order to gain access to the in- terior. No large blocks have ever entered to any great distance into the cave. Waves have no doubt thrown smaller wave- worn pebbles over the larger guarding blocks and have moved these back and forth at exceptional times, but such Plate 21 all from a photograph taken from the At a in the left upper portion we may see horizontal on which the cave was cut, shows a slight downthrow on reater part asurface produced by differential View of mouth of Darkroom cave and adjacent w lake edge on October 23, 1909. slickensides. The fault plane, the right. The wall at the right shows for the g solution. SIXTH REPORT OF THE DIRECTOR I909 187 movement has not been sufficient to effectively cut the cave walls at their level. Material of this nature is also absent from the second chamber. Late in the summer of 1909 a small excavation was made in the deposits covering the floor of the mouth of this cave. On digging down the size of the pebbles rapidly decreased, and numerous small and well polished granitics and quartzes were found among the limestone pebbles. At the depth of a few decimeters a thin layer of very fine and clean gravel was en- countered and immediately under this was a fine and well oxi- dized clay containing a few pebbles so thoroughly decomposed that the peen of the hammer easily cut them and left half of the pebble imbedded in the undisturbed clay. The boundary be- tween gravel and clay was very sharp and distinct. A block, Or a projecting edge from the cave floor, now interfered with making a deeper cut in the small place chosen. The fine oxi- dized clay and the few thoroughly oxidized pebbles speak very decidedly for a deposit at least as old as that of the Hochelagan sea. We should also state that the buried portion of the cave wall was but a continuation of the exposed portion above. The cutting of the whole cave opening was thus shown to be older than the clay filling, and all subsequent erosion has hardly modified the opening. That this cave in all its essential features is at least as old as the glacial period must be considered as demonstrated beyond the shadow of a doubt. Miscellaneous evidence. ‘To the east of this cave is another which can be reached by boat or by the sinkhole shown on plate 2. The natural bridge between the sinkhole and the lake consists of badly fractured material. About 500 pounds of this rock were recently detached from its undersurface and allowed to fall to the cave floor in order to insure the safe passage of pupils doing field work in physiography. ‘This cave is also cut along a fault plane parallel with that of Darkroom cave. One slickensided surface, by means of its well preserved diagonal lines, shows that the small vertical displacement (throw) was accompanied by a greater horizontal component. A view of the mouth of this cave has already been seen in plate 1. It is one of the few caves that have had their openings cut to the very top of the cliff. A careful examination of plate 21 will show that the same thing might easily have taken place there but for the fact that the wedge-shaped mass pinched in between the nearly parallel fissures has the smaller edge downward. In Bridge 188 NEW YORK STATE MUSEUM cave, as we shall call the one we are here discussing, there is a similar wedge-shaped mass but toward the front of the cave the edge of this wedge was uppermost. There is some evidence in this cave that solution began its work on two nearly parallel fissures which were about a meter apart near the top of the cliff but which increased this distance to a little more than 2 meters in descending to the present low water level of the lake. This partition was subsequently cut away in many places. Dentpit action is at work cutting through the separating walls of smaller contiguous caves. Portions of these former sepa- rating walls are now left as pillars supporting the roof of a widened cave mouth. This cave has two items of proof to offer concerning its age, which differ from any we have yet mentioned. Plate 22 shows a portion of the east wall of this cave in the region of the sinkhole. At (a) we have a portion of the older face of the wall removed by the action of expanding water in joint planes. The surface thus exposed is not a fresh one but has been subjected to a long period of weathering. We may note a still older sur- face of similar character under the overhanging mass at the right. At (b) we have what we may call an original surface or one not yet acted upon by the agent specified above. The deep etching which the edges of the very irregular bed surfaces have received and the much weathered edges of the finer laminae both speak of very great age, for the position is here a sheltered one. At (c) we have a portion of the wall of a cylindrical excavation which appears to have been cut by spirally descending waters. This cylinder opened into a basin which was more deeply cut in the side wall and which plainly speaks of water carrying abrading tools. Note also a portion of the deeply cut basin diagonally above this at the right which also emptied into it. Is any agent so cutting these walls at the present time? One answer to this question is to be found in the filling of this part of the cave for this filling has covered up a large portion of the lower basin and this it could not have done were any such cutting action now present. The filling is talus like and neither deposited nor modified by running water. — Another answer and yet the same, is to be found in the appearance of the surface at (c) which shows its etched, irregular bed edges and its laminae nearly as plainly as at (b). The slight difference between these two surfaces is due to the fact that the recessed surface at (c) is now better protected, from even getting wet, than is the surface at (b). The very slight drainage this cave may now receive from rainfall or melting snows has had nothing whatever View of a portion of the east wall of Bridge cave near the sink hole. From a photograph taken November 2, 1909 p i a ates anit ney Lwese t ee eh wi 4 , 4) ORT ae BRS Wn. ® we re : ; - og a . he ‘4 4 ‘ : ae 4 “ AL . a ; : ae ' t ¢ Ls 4 Pe os) ae Be att ~ t ri y ba a —_ i 4 * ‘ . é “ sy ” bh 5 5 / ley au eS - < 0 pay a a 9 n o " é « z ) ee a ait i - , 5 it , x s ) 5 ay Se > Bj. et, ; } ' a 4 “s ~ i - | t e . C ni = SIXTH REPORT OF THE DIRECTOR I909 189 to do with the erosion of the ‘arger features here shown. The large chamber of Darkroom cave shows the same type of cutting by falling and whirling waters carrying abrasive material. No water whatever now enters the upper portion of this chamber. An examination of plate 22 will show that the descending streams which must have done this work were reflected and thus turned from one place to another either along the fissure plane or from one wall to its opposite. The shallow nature of the cut at (c) and the deeper cuts at the right of it and below it are due to such reflections of the falling stream. These caves present many other examples of the same nature and the evidence, in all its varied features, is wholly against any such cutting at the present time and wholly for a cutting which must have taken place many thousands of years ago. All of the cuts and the great chamber in Darkroom cave with its horizontal and cylindrical outlet, _ point irresistibly to the conclusion that we are here dealing with glacial moulins cut in older rock fissures. This conclusion however opens up another field of great interest. At the time of the melting of the later Wisconsin ice sheet the rocks of Valcour island had been so far depressed by isostasy as to bring their highest portions below the level of the sea. If the caves had been modified by glacial drainage at that time, the waters passing through these caves must have completely filled every por- tion of them and been moved under great pressure. The leaping of such a drainage stream from side to side, cutting now more in this place and again in that (and cutting as if falling freely) would be out of the question. The effects could not have been so markedly localized as we now find them to be; but would have been of a larger and more uniform type. In order to find conditions that would yield the effects we have here noted we are compelled to go back to a time when the land was at least as high as it is at present. It is quite possible that we have in these cases a witness of moulin action at least as old as the earlier Wisconsin stage, if not older. | The next new item of proof offered by Bridge cave comes from an examination of its northward extension. The entire cave roof (the wedge between the two fissures) has been thrust down and fractured, as the result of great pressure above. A depression on the surface of the ground over the cave can be seen to run many meters to the north although now covered with soil and overgrown by trees and bushes. The only agent that could have forcefully thrust down this wedge is glacial ice. I9QO NEW YORK STATE MUSEUM A unique but important bit of evidence is found in the west wall of the narrow channel separating Spoon island from Valcour island. A rather high rocky promontory runs about east-northeast some 450 meters from the inner beach of Spoon bay. A block about 50 meters wide, cut off from the end of the promontory by a north and south fault, has been converted into an island, namely Spoon island, by erosion along the fault plane. Since the rocks dip south- erly, and as the downthrow was on the east, Spoon island has ap- parently been shifted 100 meters to the north and forms a distinct barrier to currents moving easterly along the south wall of the bay. The imprisoned glacial ice and till of the Spoon bay basin would thus find their nearest and lowest southerly outlet lying along this fault channel, which is about 30 meters wide with high and nearly vertical walls on either side. The ice and till finding its exit here would be forced through under great pressure. The northerly position of Spoon island with reference to the present end of the promontory soon allowed the till stream a free passage across the south end of the island to deeper and freer channels, and this eastward deflection was hastened by a well marked buttress on the middle of the east wall of the promontory. That this buttress has been subjected to great pressure from the north is clearly shown by nearly horizontal pressure joints which cut diagonally across the beds and curve upwards as one follows them southerly. The caves shown in plate 1o lie just south of this buttress, and they must have been protected by it in a very marked degree. The rather small and northernmost member of this series of caves is located in the base of the buttress itself, and the pressure received by its northern wall was great enough to dislodge from it a rectangular block weighing some 300 pounds and thrust it southerly and inward against a filling of till. As the bottom of this cave lies some distance below the surface of low water, while its top is completely covered by high water, the finer material of its glacial contents has been washed away. The thrust-in block, however, still holds a number of imprisoned, glaciated limestone pebbles the size of cobblestones. As the upper and narrower por- tion of this cave is thus shown to have been filled with glacial till, we are again forced to conclude that all of the caves of this series are preglacial and that they have been but slightly modified since glacial times. This cave offers very valuable evidence as to the solvent powers of Lake Champlain. Although it occurs in the purer dolomitic lime- SIXTH REPORT OF THE DIRECTOR I909 IQI stones of the Chazy beds, postglacial waters have not cut back its walls to an extent that will yet allow the removal of the impris- oned pebbles.. The block offers still more conclusive evidence, for though slight movements have enabled it to grind its own lower surface and the bed on which it rests, thus allowing water to have free access to its other surfaces, it has suffered but slight loss in size since glacial time. We have thus an additional proof which supports strongly our contention from other evidence that the pres- ent lake, through simple solution, has not removed material from its exposed limestone surfaces to a depth exceeding 3 millimeters. There is yet another aspect from which we may view this cave question. Wherever the purer Chazy beds are exposed on the sur- face of Valcour island their unfilled master joints or fissures will be found to have suffered in varying degrees by solution and chemical action at the hands of surface waters. In some places these joints have been so widened along considerable portions of their length as to freely admit the leg of a man. In other places we imay find joints whose faces seem to meet at the surface while they are separated in their deeper portions. Along such joints we find open circular holes in some instances small and close together and in other instances so large as to freely admit one’s leg. I have been told that holes of this type have sometimes broken the legs of cattle, and I have noticed that many of these have been artificially filled or covered. These dissolved joint crevices extend to depths of some 20 meters Or more (65 feet and over). In Sloop bay, where a por- tion of the north wall has been quarried, these joint openings are seen to widen out into chambers which plainly show the effect of swiftly moving waters. Such opened joints with their inner cham- bers are often accessible to foxes and many of them have been used as dens. We are now prepared to face a new problem. If our faith in the power of solution is great enough to allow us to conclude that surface drainage has accomplished all of this extensive joint open- ing since these rocks emerged from the Hochelagan sea, we must also conclude that during the longer periods of exposure which pre- ceded the approach of the Wisconsin ice sheet joint crevices would have been acted upon by similar agencies, been cut down to former base levels and widened out into chambers. far surpassing in size those now existing in this region. These two conclusions involve the making of a third as follows: To remove every trace 192 NEW YORK STATE MUSEUM of these older joint channels (for our first conclusion asserts that the present ones are all new) we must further conclude that the Wisconsin till sheet cut away the tops of these isolated limestone hills to a depth even greater than the 20 or more meters now occu- pied by the existing system of joint channels. Now this third con- clusion is one that can not be maintained and with it the first also falls. There seems to be good and abundant evidence that these hill tops were cut away by recent glacial action to a depth that rarely exceeded 2 meters, and even though we should allow more than five times that amount we should still expect to find the widened bases of the joint channels of the older period. Joint solution through the action of precipitated waters is an exceedingly slow process, and all that post-Hochelagan precipitation has been able to accomplish is a washing out of sediments accumulated dur- ing the recent period of submergence, and a very slight enlarge- ment of the older channels. As the shore line caves are for the greater part but modifications of these old joint channels the pre- glacial origin of the one implies also the preglacial beginnings of the other. The varied and cumulative evidence here presented seems to the writer to amply warrant the conclusion that both joint channels and caves are, in their larger features, preglacial. A few words concerning their origin may assist in more clearly comprehending the questions involved. Origin and development Where locally elevated regions have been unable to maintain a mantle of soil the surface rock is subjected to more rapid changes and greater extremes of temperature than where such a mantle has been allowed to accumulate. The effect of such changes tends not only to develop and maintain joint crevices, but it opens them "aut \the end of the winter’s cooling more widely and to greater depths than can occur in covered regions. At or soon after the time of widest and deepest opening the waters from melting snows and spring rains enter with great freedom, and after passing rather rapidly through them exit at lower levels thus quickly emptying _all spaces not kept full by capillary attraction. These spring waters with a temperature of nearly zero degrees would contain more abundant carbon dioxid than summer waters, for the snow mantle of winter absorbs this gas not only from the air above but from the fracture zone below. The period of widest open crevices would SIXTH REPORT OF THE DIRECTOR 1909 193 therefore coincide very closely with the period of most abundant flow of chemically active water. The deeper and narrower por- tions of crevices kept full by capillary attraction would lose no appreciable amount of water by evaporation on account of the small and protected exposed surface. Such waters while they might approach saturation would rarely reach it because each fresh filling of the space above the water surface maintained by capil- larity would add mechanical pressure and force the older water out at lower levels, thus refilling the crevice with fresh water. As the expansion of the beds during the summer heating forced the crevice walls more closely together, a portion of the water held by capillary attraction would be forced to occupy new positions and would take its dissolved load with it. Evaporation would rarely be rapid enough to allow of deposit and the occasional advent of summer rains would furnish abundant fresh water and help to remove that more nearly approaching saturation. Fall cooling and the more abundant rain of that season in this locality would be very effective agents in removing material dissolved during the summer. Exposed joint crevices, so situated as to receive surface flow, are thus gradually widened and deepened. Other joint crevices con- necting with these might not receive so much water directly from the surface but they would help to carry the subterranean flow and become also widened. As the system developed the waters would move in certain channels with greater freedom. Dust and disintegrated particles accumulating on the exposed rock surface would be swept by rainfall into these openings, and the effects of abrasion would be added to those of solution. Joint crevices thus become joint channels. As these are widened they admit the cold air of winter in greater volume and the circulation maintained at this season serves to more effectively chill the rock mass and thus open the crevices to greater depths. As these channels approach local grade (determined by the level! of a surrounding body of water or by the water table of the mantle rock flanking these regions) the deepening of the crevices ceases, but lateral cutting is continued. Such basal widening of the system is an indication of maturity. Such work must be exceedingly slow, for the water supply 1s only such as falls on the very limited area in question. The waters doing the work would be free from humus acids on account of the bare character of the rock surface. Expansion of freezing water would be effective near the surface, but the depth at which it could be considered as an important factor would be very limited. 194 NEW YORK STATE MUSEUM If the temporary base level was determined by a surrounding body of fresh water, as it appears to have been in the case of the Valoour island elevation, the exits of the joint channel system of drainage would be under the influence of a greater number of erosive agencies than the inland portions of the same system. So- lution would be incessant, the solvent would be always in motion, and it never could approach a condition near saturation. The pres- ence of light would permit the growth of lowly organized plants and animals, and their metabolic processes while living and their decay at death would both favor the process of chemical so- lution. If we will compare the effects of simple quiescent solution by thin water films approaching saturation with the effects of chemical and mechanical solution by incessantly acting and con- stantly moving waters of great volume, we shall see that this dif- ference in erosive power would of itself turn joint-channel exits into water-level caves. To this means of differentiation we must add the influence of wave motion. This agent does work of very varied ‘character from that accomplished through sliding or roll- | ing of heavy blocks or the throwing of pebbles taken temporarily into suspension, to the work of broken wave vortexes holding solid particles so fine as to be almost in a state of permanent suspension. The submerged condition of the cave floors on Valcour island has protected them from the more energetic types of wave erosion, but the effects of vortex work are very manifest. Expansion of freez- ing water in these joint-channel exits is also a factor productive of widening. Asa result of these agents of erosion the joint-chan- nel exits become caves which narrow toward their roofs and rapidly narrow to channel dimensions as they enter the rock mass. While the foregoing discussion outlines the probable history of formation of the larger shore-line caves of Valcour island, it does not account for the formation of the majority of the smaller open- ings for these do not seem to be connected with joint channels. If a narrow joint crevice, so situated as to receive little water from rainfall in its higher portions, is bathed below by lake waters, such waters will tend to fill the crevice by capillary attraction but will at the same time receive all dissolved material and tend to maintain a fresh-water filling. As the lower portion of the crevice is thus widened the hight to which the water filling 1s maintained is lessened, but a new factor comes into play, for the effect of wave pressure in filling and emptying the crevice becomes now more pronounced and allows of more rapid changes in the filling. So soon as the breach becomes wide enough to permit water vortexes SIXTH REPORT OF THE DIRECTOR 1909 195 to act on its walls, dent-pit action commences, and all other local agencies become more effective. As these caves thus work their way back from the coast line the air in them is at times compressed by storm waves which break against and cover their mouths. A large portion of this compressed air thrusts out a volume of water at the upper portion of the cave mouth with great violence, and the tops of these spouting caves are thus cut into the form of an arch. A portion of this air, however, with its contained hundreds or thousands of dust particles per cubic centimeter! must be dis- charged backward into the open joint crevice with considerable in- itial speed and thus serve to widen its proximal portions and allow freer entrance of water to these portions at times of high water. Joint channels and joint caves were more or less modified during the last glacial period. With the advent of this period the outer portions of the rock mass were gradually lowered in temperature, and a condition of permanent frost came to occupy the joint chan- nels. These were thus filled with ice before surface movement of the ice sheet became an effective erosive agent. In many locali- ties in the glaciated regions cf North America there are deep fis- sures or cavernlike openings which were so filled and which still con- tain glacial ice. The ice filling of these joint channels saved them from being filled with mantle rock when the ice movement began and saved them also from a later filling of till, though they received a till covering. The loss of material from the underside of some of these till coverings is now made manifest by a sinking surface over certain joint channels or by small sink holes like that shown in plate 6. At some time during the glacial period subglacial drainage must have been comparatively free on surfaces now some 600 feet below the highest level of Lake Vermont (Glacial Lake Champlain)? else it is hard to conceive how giant kettles and rill channels (cut by surface flow of glacial waters) could be now found in this lower region. During such a time of elevation (at least to a degree as high as the present) subglacial waters found their way into wide joint channels through narrow surface openings and these were rapidly cut into circular shape by spirally descending waters. Some of the larger caves were thus occupied for a brief period by rap- er ee i 18ee Aitken, J. On the Number of Dust Particles in the Atmosphere. Roy. Soc. Edin. Trans. 35:1 (1888) ; see also Nature, 37:428 (1888), 40:394 (1890). * See Woodworth, J. B. Ancient Water Levels of the Champlain and Hud- son Valleys. N. Y. State Mus. Bul. 84, p. 195. 196 NEW YORK STATE MUSEUM idly moving subglacial streams and their walls still show the effect of these moulins [see pl. 22]. The old relation of these joint channels surface drainage has also been in part changed by glacial erosion, for wide open chan- nels may be often found where they now receive little surface drainage, and undrained surface basins may occur at no great dis- tance from them. The movement of the till sheet along the cast and west sides of Valcour island has modified many cave mouths, cutting away more from the lower portions of their southern walls than from their northern walls and thus leaving the latter the more nearly vertical. This effect may be seen in some of the wider cave mouths shown in plate 3. A moving till sheet would also cut away more rapidly at the cave mouth level, where caves were numerous, and thus tend to leave overhanging or convex faced cliffs, such as may be found on the east side of Spoon island. During the occupancy of the region by Lake Vermont and the Hochelagan sea these joint channels and caves where not protected by an undisturbed till sheet were in part filled by fine though rather rapidly deposited sediments, and the whole tendency of these two stages was toward the preservation of the erosive work already accomplished rather than toward the inauguration of any new cut- ting of the old channels or cave recesses. With the beginning of the Lake Champlain stage these old joint channels served again, though in a modified manner, their ancient function and the lake waters began an attack on the old cave mouths. This stage has existed for so short a time, geologically speaking, that it has produced but slight changes in the character of the older features. It is becoming more and more manifest that the work accom- plished by the last glacial period, although vast and tremendously impressive, did not obliterate so much of a former surface history as many geologists have been inclined to believe. Glaciated re- gions must be likened rather to a palimpsest from which a large portion of the older story may‘be recovered, and much work in this direction remains to be accomplished. SIXTH REPORT OF THE DIRECTOR IQOQ 197 CONTRIBUTIONS TO MINERALOGY BY iH. P. WHITLOCK Brookite Indian Ladder, Albany co. Brookite from a new locality in the Helderberg escarpment was noted on a specimen of calcite collected by Mr C. A. Hartnagel. Subsequent examination of the locality resulted in the collection of a suite of specimens of calcite which yielded on solution 10 small erystals of this mineral. The calcite vein from which these were obtained is situated at a point about half way up the cliff about 2 miles south of Meadowdale and ™% mile east of the road which ascends the escarpment from the latter village. The crystals are minute, measuring from I millimeter to-.5 millimeter in length. They are in every instance brilliant, with sharp, well defined faces and in general habit resemble mpaeeicom Eilenville, Ulster co., ieee Fisute I a and b shows the prevailing crystal habit. The vertical zone is much striated, due apparently to the development of vicinal pris- Bes Je oalsie, Lulduaon, Melee matic forms. The following forms were noted on the seven crystals which were measured: mmeenc(oor), k(4i0), 1(210), m(1ro), y(104), t(o2r), eiit2)-and e(122). The following measurements served to identify the forms: LETTER | ANGLE Pe ety | 80 OF | sone | cancocanmn MEASURED | CALCULATED ss ci a ne | ee ce) / | te) / mean’: . . PLO DLO 13 99 46 | 99 50 1 ae Be S210) | ) 134 21 134 214 mek... 410 : 410 10 155 54 156 14 a a O01 : 104 a 15°, 37 15 40 tis (001: O21 | 15 6209S 62) 04} eee 12: 112 4 44 25 44 46|| a ae |g Pe By bp 6 53 44 53 484! Bee bo 122 4 19°: do 735i] ere 1222122 +) 44 19 44 a ec 198 NEW YORK STATE MUSEUM Fluorite Rossie, St Lawrence co. Among the specimens in the New York State Museum collection is one worthy of notice, collected by the late Prof. Ebenezer Emmons, from Rossie, St Lawrence co. This specimen which measures 9 by 5 centimeters consists of a mass of rhombohedral calcite on which are implanted several compound crystals of fluorite of unusual habit. These latter are built-up aggregates, roughly octahedral in shape, composed of minute individuals of hexoctahedral habit grouped in parallel position. The octahedral angles of the aggregates are in every case terminated by well developed superposed hexoctahe- dral crystals as shown in figure 2. The compound crystals are Fig.2 Fluorite, Rossie transparent, light green in color and average 15 millimeters in diameter. They are evidently of the same generation as the calcite in which they occur and are associated with chalcopyrite in well developed crystals. Measurements on three isolated crystals yielded the following forms: ‘a( 100), ,o(111), \ v(731). and SIXTH REPORT OF THE DIRECTOR 1909 199 @(19.1.1 ). .The last is new to the species. The faces, with the exception of those of o(111), are sharp and brilliant. The planes of the new trapezohedron @(19.1.1) show a slight tendency to de- velop unsymmetrically in opposite pairs with respect to the axes of tetragonal symmetry. In several instances reddish violet spots of cubic outline were noted in the center of the hexoctahedral crystals. The following measurements served to identify the forms Mizar) and ©(10.1.1): NUMBER OF LETTER ANGLE Ae MEASURED | CALCULATED i [e) / (@) / 7 a fol (13 4 OREO OH Lae Ls Renee ak. Holes it 5 amare © 14° 57 Vs: Foleo 4 Ae 5 43 122 5) a 110)0 ra en ae | 4 4 13 Aes Magnetite Split Rock, Essex co. Among the specimens collected in the summer of 1907 by Prof. James F. Kemp of Columbia University, was one from the Split Fig. 3 Magnetite, Split Rock Rock iron mine which proved to be of special interest. Through the courtesy of Professor Kemp this specimen has been placed at 200 NEW YORK STATE MUSEUM the disposal of the writer for study. The specimen consists of a mass of titaniferous magnetite forming portion of a joint plane in the ore body. The surface of the joint is covered with small crystals of magnetite of cubic habit closely associated with werner- ite in small transparent crystals. The comparative rarity of the cubic crystal habit in connection with magnetite’ together with the adaptability of these crystals to measurement, has rendered advis- able the following brief note: The magnetite crystals which average 2 millimeters in diameter are exceptionally brilliant, well developed and free from distortion. The simpler combination which is shown in figure 3 consists of the cube a(100) developed to a dominant crystal habit and modified Fig. 4 Magnetite, Split Rock by the octahedron o(111) and the dodecahedron d(110), both of these latter forms being present in small development. A more complex combination is shown in figure 4 and consists of the above forms developed to about equal habit and modified by the trigonal trisoctahedrons q(331) and k(552) and by the new trapezohedron YY —707==(711). They lie well in zone, the faces of the trigonal trisoctahedrons and of the dodecahedron being markedly striated parallel to the zone [100.110]. The planes of the trapezohedron w(7I1) are small but extremely bright and give excellent reflec- tions. The forms were identified from measurements obtained from five of the best crystals. *Magnetite crystals of cubic habit were noted by H. Sjogren from Mossgrufva, Nordmark. Bul. Univ. Upsala. 1894-95. 2.63. SIXTH REPORT OF THE DIRECTOR I9QOQ 201 NUMBER OF LETTER ANGLE eae MEASURED | CALCULATED ce) / (e} 7 eee... ies (GNI 12 ae le) 35 16 i Sa ie shoe 8 22 OT fle 22°70 eek. 2... Piles 255 a LO A 19 28 eee... mea 7 L 2 Gee e.2 LOG ets... BOO} AL 12. 1 Meat 11 25% Gypsum Garbutt, Monroe co. Among a number of specimens collected in the spring. and summer of 1909 from the gypsum region of western New York by Mr Henry Leighton, assistant in economic geology, was a suite of I2 specimens of crystallized gypsum which furnished crystals compara- tively rich in forms. The specimens in question were collected from the mine of the Garbutt Gypsum Co., and from No. 2 mine of the Lycoming Calcining Co., both situated at Gar- butt, Monroe co. The gypsum crys- tals occur in narrow seams in massive gypsum and are sometimes associated with crystalline sulfur of remarkable purity and transparency. The crys- tals are colorless, transparent and average 5 millimeters in length paraliel to the positive unit pyramid. In crystal habit, they conform closely to the type shown in figure 5. The prismatic zone is particularly rich in forms, yielding 8 of the 12 prisms re- corded for gypsum.t Two rare neg- ative pyramids in the zone [oro.1o1] were noted, present either together or alternating on all 12 of the crystals measured. These "Goldschmidt, V. Krystallographische Winkeltabellen. Berlin 1897. Luedecke, O. Minerale des Harzes. Berlin 1896. 377. wO2 NEW YORK STATE MUSEUM gave goniometer readings which corresponded to the indexes (212) and (g13). The letters o==(g12) and p—(s13) have been as- signed to these forms. The distribution of the occurring forms is as follows: CRYSTAL LETTER | SYMBOL Te) TE 1 Pave) Ve) Vn Va VX |e | tee yn caeiaee OG - | e.AN ce aaa ae ee > a eres eased. x )| Soeslee | oPaapastets tate OK O ae to-oeml to-cii hee all >-a eo eal eallino-emml-celorap sc | 3c | Te Firat er Re SRO) ea hes see | sec poXaae | XC | EXC IN raha mo Sy Chg DSS anes QAO Se ea AIS Re oe OK, axe ae ea A Ok ie Ser B20 tue eee eee SCP gs ep. 0 eee lenee ol 1s eee DUO: |e ee eee |x | Sea Saree ZOO 2 onl eel eae oc cf Se ane al tee Eo 5 x |e Oi Sok Ronee B50 ois Sie eee Scale eae eee dean alee | Rae aoe. 1 ZO oa eee exe ht 7X X | ee ee | eater Se SO hee eee eee XC oi | OR le er Nt sae eee WW1)/x|/xiJxixilxilx/xix/x/x|/x/x TG kc Oe Ka We ae elec lhc] es oe poem en anion yc |) 3c Olu eee PA Ani aud beep he ih | xe 3c Sc af ae oe a ote Wig eee Dill. (nex > aie Wee x X | K eae The following measured angles served to identify the forms; the theoretical angles are caiculated from the elements given by Beckenkamp? and adopted by Goldschmidt in his Krystallographische Winkeltabellen. a:b 1@ == O Ala sst 016505 8 ea 9S 50/., Summary of measured and calculated angles NUMBER OF ; : LETTER ANGLE ane arene MEASURED | CALCULATED 1) / [e) / ita e 101 = 100 5 90 4 90:50 DOT Re eo LOM 8 10 edey lal Ti es SU eee LOD 200 17 (Metts 7. Mele b SEN 1013320 5) 65 41 65) en ~Zeitschr. 4. Kryst.) 1862. sores e SIXTH REPORT OF THE DIRECTOR IQOQ 203 Summary of measured and calculated angles— (continued). NUMBER OF LETTER ANGLE cu ane MEASURED | CALCULATED i: 2 a OES SHO) 16 55 48 55 443 ee... LO 230 2 44 464 44 234 Page... LOM 350 2 41 534 41 224 an O20 14 36 35 ORNL 2 a Ot S130 4 ZOU Oe PAG i ees. . BOs Al G Lose ek (A Sl) ees... . ONG stat 20 69 194 69 204 ee Os... LOW 212 12 GQ We ag Oe: ea... LOL 313 13 Sones 82 50 | aa Or + 49 12 49 16 ete. Cs al 5 59 «4 58 59 a 310.: 313 5 64 584 64 55 204. NEW YORK STATE MUSEUM THE IROQUOIS AND THE STRUGGLE FOR AMER ADDRESS BY ELIHU ROOT, SENATOR FROM NEW YORK, AT THE TERCEN- TENNIAL CELEBRATION OF THE DISCOVERY OF LAKE CHAMPLAIN,? It is no ordinary event that we celebrate. The beauty of this wonderful lake, first revealed to the eye of civilized man by the visit of Samuel de Champlain three hundred years ago; the powerful personality, noble character, and romantic career of the discoverer ; the historic importance of this controlling line of strategic military communication, along which have passed in successive generations the armies whose conflicts were to: deter- mine the control and destinies of great empires ; the value to Canada and to the United States of this natural pathway of commerce; the growth and prosperity of the noble states that have arisen on the opposing shores; their contributions to the wealth of mankind, to civil and religious liberty, to the world’s progress in civilization — all these, withdraw the first coming of the white man to Lake Champlain from the dull and uninteresting level of the common- place, while comparative antiquity, so attractive and inspiring to the people of the New World, lends dignity and romance to the figures and the acts that have escaped oblivion through centuries. Even a dull imagination must be stirred as it dwells upon the influence which the events ‘attending the discovery were to have, upon the issue of the great struggle between France and Great Britain for the control of the continent; the struggle between the two white races for the opportunity to colonize and expand, and between the two systems of law and civil polity, for the direction and development of civilization among the millions who were to people the vast region extending from the Atlantic to the Pacific and from the Rio Grande to the frozen limits of the north. Authentic history records that late in June 1609 Champlain, ac- companied by several white companions and by a great array of Algonquin Indians of the St Lawrence valley, left the French station on the site of the old Indian village of Stadacona, where now stands the city of Quebec, upon an expedition intended by the * This illuminating address, publicly given before a distinguished audience, at Plattsburg, July 7, 1909, is here reprinted in order to give it as wide circulation as possible among the people of the State. SIXTH REPORT OF THE DIRECTOR IQOQ 205 Indians for war and by the whites for exploration. They pro- ceeded in canoes up the St Lawrence and turned south into the Richelieu, andi in the early days of July after many vicissitudes and the desertion of the greater part of the Indians they dragged their canoes around the rapids of the river and came to the foot of the lake on whose shores we stand. They proceeded up the lake with all the precautions of Indian warfare in an enemy’s country. As they approached the head of the lake they rested concealed by day and urged forward their canoes by night. At last, in this month of July three hundred years ago, they came upon a war party of the Iroquois. Both parties landed in the neighborhood of the present Ticonderoga and with the coming of the dawn joined battle. Pro- tected by the light armor of the period Champlain advanced to ‘the front in full view of the contending parties, and as the Iroquois drew their bows upon him he fired his arquebus. One of his white companions also fired. The Iroquois chief and several of his war- riors fell killed or wounded, and the entire band amazed and terror stricken by their first experience with the inexplicable, miraculous and death-dealing power of firearms fled in dismay. They were pursued by the Algonquins, some were killed, some were taken prisoners, and the remainder returned to their homes to spread through all the tribes of the Iroquois the story that a new enemy had arisen bringing unheard of and supernatural powers to the aid of their traditional Algonquin foes. The shot from Champlain’s arquebus had determined the part that was to be played in the ap- proaching conflict by the most powerful military force among the Indians of North America. It had made the confederacy of the Iroquois and all its nations and dependencies the implacable ene- mies of the French and the fast friends of the English for all the long struggle that was to come. A century or more before the white settlement five Indian na- tions of the same stock and language under the leadership of ex- traordinary political genius had formed a confederacy for the preservation of internal peace and for common defense against external attack. Their territories extended in 1609 from the St Lawrence to the Susquehanna; from Lake Champlain and the Hud- son to the Genesee, and a few years later to the Niagara. There dwelt side by side the Mohawks, the Oneidas, the Onondagas, the Cayugas and the Senecas in the firm union of Ho-de-no-sau-nee — the Long House of the Iroquois. The Algonquin tribes that surrounded them were still in the lowest stage of industrial life and for their food added to the 200 NEW YORK STATE MUSEUM spoils of the chase only wild fruits and roots. The Iroquois had passed into the agricultural stage. They had settled’ habitations and cultivated fields. They had extensive orchards of the apple, made sugar from the maple and raised corn and beans and squash and pumpkins. The surrounding tribes had only the rudimentary political institution of chief and followers. The Iroquois had a carefully devised constitution well adapted to secure confederate authority in matters of common interest, and local authority in matters of local interest. Each nation was divided into tribes, the Wolf tribe, the Bear tribe, the Turtle tribe, etc. The same tribes ran through all the nations, the section in each nation being bound by ties of con- sanguinity to the sections of the same tribe in the other nations. Thus a Seneca Wolf was brother to every Mohawk Wolf, a Seneca Bear to every Mohawk Bear. The arrangement was like that of our college societies with chapters in different colleges. So there were bonds of tribal union running across the lines of national union, and the whole structure was firmly knit together as by the warp and woof of a textile fabric. | The government was vested in a council of fifty sachems, a fixed number coming from each nation. The sachems from each nation came in fixed proportions from specific tribes in that nation; the office was hereditary in the tribe; and the member of the tribe to fill it was elected by the tribe. he sacktems of each mation governed their own nation in all local affairs. Below the sachems were elected chiefs on the military side and Keepers of the Faith on the religious side. Crime was exceedingly rare; insubordination was unknown; courage, fortitude and devotion to the common good were universal. The territory of the Long House covered the watershed between the St Lawrence basin and the Atlantic. From it the waters ran into the St Lawrence, the Hudson, the Delaware, the Susquehanna and the Ohio. Down these lines of communication the war.parties of the confederacy passed, beating back or overwhelming their ene- mies until they had become overlords of a vast region extending far into New England, the Carolinas, the valley of the Mississippi and to the coast of Lake Huron. They held in subjection an area including the present states of New York, New Jersey, Pennsylvania, Delaware, Maryland, Ohio, Kentucky, West Virginia, Northern Virginia and Tennessee, and parts of New England, Illinois, Indiana, Michigan and Ontario. Of all the inhabitants of the New World they were the most terrible SIXTH REPORT OF THE DIRECTOR 1909 207 foes and the most capable of organized and sustained warfare, and of all the inhabitants north of Mexico they were the most civilized and intelligent. The century which followed the voyages of Columbus had been for the northern continent a period of exploration and discovery, of search for gold and for fabulous cities and for a passage to the Indies, of fugitive fur trade with the natives, of fisheries on the banks and of feeble, disastrous attempts at occupation, but not of permanent settlement. Ponce de Leon and De Soto and Verazzano, Cartier and the Cabots and Drake and Frobisher and Gilbert and Gosnold, had brought the western coast of the Atlantic out from the mists of fable, but they had left no trace upon its shores. Jean Ribaut and his French Huguenots had attempted to do for their religion in Florida what the Pilgrims did in the following century on the coast of Massachusetts. but their colony was destroyed with incredible cruelty in the name of religion by the ferocious Spaniard, Menendez, and the colony of Menendez was in turn destroyed by the Gascon de Gourgues, save a feeble remnant on the site of St Augustine. Raleigh with noble constancy and persistency had wasted his fortune in repeated and vain attempts to establish a colony in Virginia. On the sites of the modern Quebec and Mon- treal, at Tadousac, at the mouth of the St Croix and at Port Royal, Jacques Cartier and Roberval, Pontgravé and De Monts, Poutrin- court and Lescarbot had seen their heroic and devoted efforts to establish a new France brought to naught by cold and starvation and disease. In that month of July 1609 in all the vast expanse between Florida and Labrador no settlement of white men held its place or presaged the coming of the future multitude save at James- town behind the Capes of Virginia, where Christopher Newport’s handful of colonists had barely survived two years of privation, and at Quebec, where the undaunted Pontgravé and Champlain only one year before had again gained a foothold. At Jamestown the mournful record of the winter of 1609 to 1610 shows us that in the spring but sixty of the colonists were living. At Quebec twenty- eight Frenchmen with Champlain had braved the rigors of a Can- -adian winter, and in the spring of 1609 but eight remained alive. In this same month July 1609 the Half Moon of Henry Hudson was repairing damages in Penobscot bay after her voyage across the Atlantic, and preparing to sail on to the noble river that still bears her commander’s name. The field was open; the hands upon the margin that reached out 208 NEW YORK STATE MUSEUM to grasp control seemed few and feeble, but the period of prepara- tion was past. The mighty forces that were to urge on the most stupendous movement of mankind in human history had already received their direction. The time was ripe for the real conflict to begin, and it had its momentous beginning when the chief of the Mohawks fell before the arquebus of Champlain at Ticonderoga. The conditions which limited the powers and directed the pur- poses of the various countries of Europe in the early years of the seventeenth century made it inevitable that the struggle for Ameri- can control should ultimately become a single combat between France and Great Britain. It is true that Spain had overturned the tribal government of the Aztecs and held possession along the northern shores of the Gulf of Mexico, a vantage ground from which she might well have pressed to the northward successful plans of occupation. But Spain had no such plans. When the search for treasure had failed, and it was plain that no more Perus and Mexicos were to be found, the dark forests of the north Atlantic offered no attractions to the Spanish Conquistadores who sought the spoils of conquest rather than the rewards of labor. With the death of Philip the Second the decline of Spanish power had already begun. His successors were feeble and incapable. The stern, repressive and despotic control over body and soul effected by the union of military and religious organization during the first century of United Spain was accompanied by a marvelous efficiency and energy that made Spain for a time the foremost maritime and colonizing power of the world. The price of that efficiency, how- ever, was the loss of the only permanent source of national energy, the independence and free initiative of individual character among her citizens. Thenceforth Spain was no longer to sway the rod of empire, but holding it weakly in feeble hands was to lose one by one the world-wide possessions of Charles the Fifth and Philip the Second, until the time when the penalty of her national sin against civil and religious freedom should have been paid and the native strength and nobility of her character should be able to reas- sert themselves in a period of renewed growth and: reestablished power and prosperity; a time which we hope and trust has already come. Portugal, still clinging to the fruits of her explorers’ genius, and sturdy Holland, strong in her newly won freedom, were looking not to North America but to Brazil and to the Orient for their opportunities to expand, and the future colony of New Amsterdam SIXTH REPORT OF THE DIRECTOR I909 209 was destined to be readily transferred to the English for the sake of greater opportunities to the Dutch East India Company. Germany was not yet a maritime power. Loosely compacted under the failing hegemony of the House of Austria she was upon the threshold of the Thirty Years’ War, in which the most fright- ful slaughter and devastation were to destroy her cities, lay waste her fields, reduce her population from thirty millions to twelve mil- lions, and set back her civilization for centuries. Into that vortex of destruction Sweden also was about to be drawn, and her forces were to be engrossed in the struggle for national existence, so that the hopes of Gustavus Adolphus for a New Sweden upon the banks of the Delaware were to fail of fruition, and the Swedish colony in America was to pass with _hardly a struggle into the hands first of the Dutch and then of the English. : | Prussia was a dependent dukedom. Russia had still three quarters of a century to wait before Peter the Great was to begin to lead her from semibarbarism into the ranks of civilized powers. . Italy was a geographical expression covering a multitude of petty states. Of all the peoples of Europe, only the French and the English possessed the power, the energy, the adventurous courage, the op- portunity and the occasion for expansion across the Atlantic. The field and the prize were for them and for them alone. Upon the throne of France was Henry the Fourth, the greatest of French kings. In the governing class of Frenchmen, political and religious, were the virile strength, the intellectua! acumen, the romantic chivalry, the strong passions, the love of glory, the capac- ity for devotion to ideals, which were to make possible the rule of Richelieu, the ascendancy of Louis the Fourteenth, the political idealists of the Eighteenth century, the tremendous social forces whose outbreak in the French Revolution appalled the world, and the armies of Napoleon. In England the reign of great Elizabeth had just closed. It was the England of Spenser and Shakspere and Bacon; of Cecil and Raleigh; of Drake and Frobisher. John Hampden and Crom- well and Milton were in their childhood. For four centuries since Magna Charta, Englishmen had become accustomed to the asser- tion of the individual rights of the citizen against arbitrary power. Since the repudiation of Roman supremacy over the national church by Henry the Eighth three generations had become wonted to. the assertion of religious freedom. King James’s translation of the 210 NEW YORK STATE MUSEUM Bible was in progress and nearly completed. The deep religious feeling of the Puritan reaction against both Roman and royal epis- copacy that was to cost Charles the First his life and James the Second his throne had already become a controlling motive among a great multitude of the English people. From these two countries, each possessed of great powers, each endowed with noble qualities, proceeded. the colonists who were to dispute for the possession of America. The French movement was in the main governmental, aristocratic, proceeding from state and church, designed to extend and increase the power, dominion, and glory of the king, to convert the Indians to the true faith, and to extend over them and over all the lands through which they roamed, and over all who should come after them and take their place, the same iron rule of conformity against which the Huguenots of France were vainly contending. The English movement was in the main popular, proceeding from the people of England who wished to escape either church or state at home and to find freedom in a new world for the practice of their religion or the pursuit of their fortunes according to their own ideas. Some of the English colonies braved the hardships of exile rather than conform against their consciences to requirements of practice and doctrine which the English church imposed. Some sought for fortune in the New World because the state had so distributed the property and so closed the avenues for advancement in England that they must needs seek opportunities elsewhere if at all. For centuries the struggle between civil and religious absolutism on the one hand and individual liberty on the other were waged alike in France and England. The attempt to colonize America came from one side of the controversy in France and from the other side of the same controversy in England. The virtues of the two systems were to be tried out and the irrepressible conflict be- tween them was to be continued in the wilderness. For capable and efficient leadership, for farsighted and compre- hensive plans, for clear understanding of existing conditions and prevision as to the future, for conspicuous examples of heroic achievement and self-devotion, the palm must be awarded to the French over their English competitors. There are few chapters in history so full of romantic interest, so compelling in their de- mands for sympathy and admiration, as the record of the century and a half that began with the wooden fortress of Champlain under the bluff at Quebec and ended with the fall of Montcalm on the Heights of Abraham. SIXTH REPORT OF THE DIRECTOR I9OQ 2I1 The world owes many debts to France. Not the least of these is the inspiration the men of every race can find in the noble ex- amples of such explorers as Niccolet and Joliet and La Salle: such leaders as Champlain and Frontenac and Duquesne and Mont- calm; and such missionaries as Le Caron and Breboeuf and Mar- quette. They strove for the execution of a great design, holding hardship and suffering and life of little account in their loyalty to their religion and their king. With infinite pains they won the friendship of the Indians of the St Lawrence and the far North- west; they carried the flag of France to the mouth of the Missis- sippi; they drew a cordon of military posts up the St Lawrence across to the Mississippi and down to the Gulf, well designed to bar the westward advance of the English colonies, to save the great West for their race and thence to press the English backward to the sea. Their soldiers were, as a rule, better led, better organized, and moved on more definite and certain plans than the English. Oc- casionally some born fighter on the English side would accomplish a great deed, like Pepperell at Louisburg, or some man of supreme good sense would bring order out of confusion, as did Franklin and Washington, but as a rule colonial legislatures were slow and vacillating, colonial governors were indifferent and shortsighted, and colonial movements were marked by a lack of that definite re- sponsibility, coupled with power, so essential to successful warfare. Fortunately for England, between the two parties all along the controlling strategic line from this Lake Champlain to the gateway of the West at Fort Duquesne, stretched the barrier of the Long House and its tributary nations. They were always ready, always organized, always watchful. They continually threatened and fre- quently broke the great French military line of communication. Along the whole line they kept the French continually in jeopardy. Before the barrier the French built forts and trained soldiers — be- hind it the English cleared the forests and built homes and cultivated fields and grew to a great multitude, strong in individual freedom and in the practice of self-government. Again and again the French hurled their forces against the Long House, but always with little practical advantage. At one time De Tracy, the Viceroy, burned villages and laid waste the land of the Iroquois with twelve hun- dred French soldiers. At another De La Barre, the Governor, with | eighteen hundred; at another De Nonville with two thousand; at another Frontenac with six hundred; at still another, Frontenac 212 NEW YORK STATE MUSEUM with a thousand. Always there came also a cloud of Algonquin allies. Always the Iroquois retired and then returned, rebuilt their villages, replanted their fields, resumed their operations and in their turn took ample revenge for their injuries. So, to and fro the war parties went, harrying and burning and killing, but always the barrier stood, and always with its aid the English colonies labored and fought and grew strong. When the final struggle came between the armies of France and England, the French had the genius of Montcalm and soldiers as brave as ever drew sword; but behind Wolfe and his stout English hearts was a new people, rich in supplies, trained in warfare and ready to fight for their homes. South Carolina, the records show, furnished twelve hundred and fifty men for the war; Virginia, two thousand ; Pennsylvania, two thousand seven hundred; New Jersey, one thou- sand; New York, two thousand six hundred and eighty; New Hampshire and Rhode Island, one thousand; Connecticut, five thou- sand; Massachusetts, seven thousand. It was not merely the army —it was that a nation had arrived, too great in numbers, in extent of territory, in strength of independent, individual char- acter, to be overwhelmed by any power that France could possibly produce. The conclusion was foregone. A battle lost or won at Quebec or elsewhere could but hasten or retard the result a little. The result was sure to come as it did come. | In all this interesting and romantic story may be seen two great proximate causes of the French failure and the English success; two reasons why from Quebec to the Pacific we speak English, fol- low the course of the common law, and estimate and maintain our rights according to the principles of English freedom. One of these was the great inferiority of the Indian allies of the French, and the great superiority of the Indian allies of the Eng- lish; the effective and enduring organization, the warlike powers, of the Iroquois, and their fidelity to the “covenant chain” which bound them to our fathers. The other cause lies deeper: It is that peoples, not monarchs, settlers, not soldiers, build empires; . that the spirit of absolutism in a royal court is a less vital principle than the spirit of liberty in a nation. In these memorial days let there be honor to Champlain and the chivalry of France; honor to the strong free hearts of the common people of England; and honor also to the savage virtues, the cour- age and loyal friendship of the Long House of the Iroqouis. | aur wen re poe a ae 1M, Wr wrt et Ae ma joles”" es Pie me ok AG f we sheng y me Yue a . ~+ deel _ 1 - A, al ae os ch) t UNIVERSITY OF THE STATE OF NEW YORK JOHN M. CLARKE DIRECTOR STATE MUSEUM BULLETIN 140 PLATE 1 ® ») () st a OW THT Git: Ip Heaegiy ; / i} 2 (i W W mara b. 3 \ r & 5) Karey: eS) \ On +,+ ashe 4 a uy I is ig aN IN Pp NY aS = J SS ee Gin, = Gra XC fi NG. LZ ae va~ TLS Cr WEA ES mt CAA mW Ge BAT EX YS OAS 8 Se THE INDIAN VILLAGE NUNDAWAO SIXTH REPORT OF THE DIRECTOR IQOQ 213 NUN-DA-WA’ -O, THE OLDEST SENECA VILLAGE ENG, Des De LOT TER Ge-nun-de-wa, or Bare hill, on the east side of Canandaigua lake 5 miles from the head, is the legendary birthplace of the Seneca nation, the place where the Nun-da-wa-o-no or “ Great Hill people ” of the Iroquois Indians held their first council fire. Its summit is 865 feet above the lake. At the south is Vine valley, separating it from a larger hill that rises 1200 feet from the lake with a steep acclivity and extends into the swamp half a mile beyond the head. This larger hill is 4 miles long and 3 miles broad at the base, the deep valley of West river lying on the east side. Though its summit is not the highest in this region, its configura- tion and surroundings make it, perhaps, the most prominent feature in the topography of the Canandaigua lake valley and its name Nun-da-wa’-o (Great Hill) strikingly appropriate. Canandaigua lake extends in a southwesterly direction about 6 miles beyond the present head of the lake. For 2 miles from the head the bottom of the valley is a sparsely timbered, flaggy swamp through which flows Naples creek, the principal inlet of the lake, a deep sluggish stream 30 to 50 feet wide, navigable for rowboats for about 2 miles. Next south of the swamp lie the “ flats,” an alluvial plain nearly a mile wide at the north end but coming to a point at the foot of Hatch hill directly opposite the village of Naples. Here the Naples creek leaves the base of the hill and takes its course diagonally across the valley for 1% miles, thence northward along the foot of West hill to the swamp. A smaller stream takes the drainage from Hatch hill and flows along the east side of the valley for 1% miles, then, after joining the Parrish gully stream crosses the flat to the main inlet not far from the south edge of the swamp, the two streams thus nearly inclosing an area of rather more than a square mile of land. Indian relics are common on a large part of this area, and in two localities their abundance and character are evidences of long or repeated occupation as the site of a village of considerable size. Conditions were exceedingly favorable for the Indians mode of life here. Except the continuation of the valley to the lake at 214 NEW YORK STATE MUSEUM the north and the West river valley at the northeast, the flats are entirely surrounded by great hills, Hatch hill at the east, Knapp hill and Pine hill at the south, and High point, West hill and Gannett hill on the west are all 1300 to 1500 feet higher than the bottom of the valley, while passes between them at the hight of about 700 feet make neighboring valleys accessible. The villages were not only sheltered from the winter storms by these hills; they were also so secluded that, though in the heart of the Seneca country and on the principal trail leading from Kanadesaga to the Cohocton and Canaseraga valleys, neither De Nonville’s invasion of their territory in 1687 nor Sullivan’s puni- tive raid in 1779 reached them. The slopes of the hills, cut by numerous gullies and large ravines, and the swamp must have afforded game in abundance. The lake was easily reached by canoe down the inlet or along the foot of West hill, while nuts and berries and the sugar maple trees grew everywhere. The soil, a dark mellow, rich alluvium, required but little culti- vation to produce large crops of fruit, corn and vegetables, and several large springs furnished an ample supply of pure water. Little can be ascertained in regard to the Indian occupation of this valley previous to the advent of the white settlers. On Pouchot’s map of 1758 the number 28 indicates a village here with the name Kanentage. Dr Beauchamp says this means “ Canan- daigua, but at the wrong end of the lake.” The dotted line show- ing Pouchot’s route, however, passes through this valley [see N. Y. State Mus. Bul. 78]. Lewis H. Morgan in The League of the Iroquois 1851, describes the separation of the Iroquois into the Five Nations and says [page 6, Dodd, Mead & Co. 1904]: “ The Cayugas and Senecas were many years united and resided upon the Seneca river, but one band of them having located upon the east bank of Cayuga lake grew up in time to a distinct nation; while the residue, pene- trating into the interior of western New York, finally settled at Nun-da-wii’-o at the head of Canandaigua lake and there formed the nucleus of the Seneca nation. The Onondagas have a legend that they sprang out of the ground on the banks of the Oswego river; and the Senecas have a similar legend that they sprang out of the ground at Nun-da-wa’-o.” On page 48 he says: “The Sen- ecas called themselves the Nun-da’-wa-o-no’ which signifies the great hill people.’ Nun’-da-wa, the radix of the word, means ‘a SIXTH REPORT OF THE DIRECTOR I9Q09 215 great hill’ and the terminal syllables ‘o-no’ convey the idea of ‘people.’ This was the name of their oldest village, situated upon a hill at the head of Canandaigua lake near Naples where, accord- ing to the Seneca legend, they sprang out of the ground.” On the map accompanying the book, the site of the village of Nun-da-wa’-o is located precisely on that part of the Naples flats where evidences of the former existence of an Indian village are now found in greatest profusion. Though flints are occasionally found on the hillsides, and very rarely a pestle, nothing to indicate an Indian village has yet been discovered in the region about the head of Canandaigua lake except in the valleys. | The late Miss Jane Mills, who during many years collected ma- terial for a history of Naples, getting much of her data from descendants of the pioneer settlers, says in her unpublished manu- script: “they (the first comers) arrived at the village of Nun-da- wa’-o.” French’s Gazetteer of New York, page 407, note, says: “ Naples was called by the Indians Nun-da-wa-o.” There is not much room for doubt that the village on the flats was the traditional Nun-da-wa-o, but it was not unusual for Indian villages to have two or more names, and we find that the pioneers and their descendants have preserved another name for this one. This valley was in the central part of the Phelps and Gorham Purchase of 1787, the Indian title to which was extinguished in 1788. In 1789 the present township of Naples was sold to a com- pany of Massachusetts men and surveyed by a party of six men from that state. So far as can be ascertained these were the first white men, except Pouchot, who arrived at this Indian village. In an address before the Naples Lyceum in 1831 the speaker, whose name is not known but who claimed to have derived his information from one of these surveyors, said: ‘‘ They entered the inlet that flows through this valley and came on shore at the old Indian landing 2 miles below the village of Naples. Here they found an Indian settlement which in the dialect of the natives was called Ki-an-da-ga, said to mean ‘between the hills.’ There resided here at this time 30 to 40 families embracing about 100 souls and from the contiguity of ancient fortificationst it may be presumed that these natives had been lords of the soil from time immemorial.” 1 . . - . . Nothing more is known of fortifications here. 216 NEW YORK STATE MUSEUM The late Seymour (A) Sutton oi Naples piblished imaimecn a series of articles entitled the Annals of Naples in which he states that the first party of settlers came up the lake on the ice in Feb- ruary 1790 and “ moved up the inlet till they arrived at a wigwam where they sought the hospitality of the Indian owner, while the cattle were turned out to feed on the tall dry grass that grew in the valley of Koyendaga. On the succeeding morning they saw the smoke of 40 wigwams against the sky and the Indians began to assemble in small groups to view the white intruders. Hiotonta in the native dignity of a chief of gigantic stature and graceful manners, and Canesque (Ka-nes-ka?) the tall and venerable ex-chief of a hundred winters, also comes to look. ‘The lofty hills,’ says Parrish (one of the first settlers) ‘on either side of Koyendaga were so destitute of timber that a deer might plainly be seen from one extreme end to the other, even to the very top.’ | At this time the Indians cultivated a large portion of the land along the creek. The flats were interspersed with patches of wild plum and the dry land sparsely covered with black walnut and sugar maple trees.” Although the Indians had surrendered all claim to the land, they had reserved the right to hunt and fish here for 20 years, and many of them remained and appear to have lived on the. most amicable terms with the settlers. : Even after they had removed to the reservation on the Gen- esee river, they returned annually during the hunting season. The late Col. N. W. Clark could remember seeing their group of wig- wams near where the Methodist church now stands in Naples village. They assisted the first settlers in their construction of a hominy block or stump mortar, the pestle or pounder of which was operated by aid of a spring pole, and took their turn in the use of it. Sutton relates some later incidents connected with the Indians here: “They were in the habit of visiting Squakie hill near the Genesee river. Canesque was there and, dying of old age, he desired to be brought back to Koyendaga to die and be buried with those he loved. In the winter of 1794 two Indians, from sympathy and kindness, conveyed the aged chief on a sled over 40 miles to the place where he chose to die. The whites ad- ministered to his comfort till he died. . - His funeral was SIXTH REPORT OF THE DIRECTOR I9QO0Q 217 ie itst attended here by the settlers.” The place of his burial is not known. “In the fall of 1796 several young Indians joined m@ewsettiers in a panther hunt in a large ravine south of the settlement, now known as ‘Tannery gully.’ The winter of 1797-98 was uncommon for the depth of snow. The Indians could not hunt even with snowshoes and were re- duced to the verge of starvation and were frequently supplied with provisions by the settlers. On a certain day the Indians assembled at a point now in the southern part of the village of Naples and after a basswood tree had been cut down the tall chief Ov-is-o-ti-ka mounted the stump. The Indians silently sur- rounding the chief with their rifles pointing up as in an act of presentation, remained in silence while the chief addressed them with an eloquence and dignity of manner which seemed to impress them and arouse their feelings. At the close of this Epece@ the teport of the rifles told the end-of the conference and the Indians quietly departed to their homes. In the autumn of 1798 the Indians held a grand festival on the higher ground a mile southwest of their larger village, hav- ing assembled from a great distance, all dressed in their neatest imanmer latee fre had been built the night before. The Indians stood in small groups. The squaws were sitting quietly on the ground, the little papooses lashed to the board were set up against the trees. At a given signal the Indians joined hands in one grand circulade (sic) and danced around the fire, rattling small sticks, beating small drums and singing in a loud monot- onous tone, giving great emphasis to the last word of each ‘strain. The squaws were in their best attire, with fur hats with silver bands and with numerous bells and hawks’ claws, beads and shells hanging from their blankets. The Indians had many gaudy trinkets and trappings peculiar to their taste and their clinking sound seemed to harmonize with their wild music. The chief Onisotika presided.” At the time Mr Sutton wrote the Annals there were living in the vicinity several sons and daughters of the pioneers and it was from them that he derived his information. In a centennial address delivered in 1889 by Hon. E. B. Pottle, grandson of one of the first settlers, he described their journey Oven tic ice on the lake and up the inlet.“ until, as they in after years said, they reached the lower Indian village. This was on what is now my farm, the upper Indian village being south of the road across the flats on lands now owned by Ira C. Williams.” 218 NEW YORK STATE MUSEUM The localities specified are approximately those where relics have recently been found in greatest profusion. _ The lower village which apparently was much the larger, was not situated directly upon the banks of the inlet but mainly along the east side of the outlet of a large spring now known as the “ Barber spring” and extending east and south to the vicinity of other springs. ‘The upper village was about 34 mile further south and bounded on the east by the “old creek” but appears not to have extended to the Naples creek on the west. All except about 1 acre of this site is covered by a heavy turf and its full extent is not known. | Evidences of occupation have also been found on the east side of the “old creek” and on the north side of the alluvial cone at the mouth of Parrish gully and west of Naples creek on the higher ground in the vicinity of the old cemetery. If any place was specially set apart by the Indians as a bury- ing ground the locality is not certainly known though it is traditional that the old cemetery in the northern part) otmame village of Naples was an “Indian burying ground” before the whites appropriated it. : Skeletons supposed to be those of Indians have been exhumed near Academy street and one of a man buried in a sitting posture and facing toward the east was found in 1907 in “ Woodchuck knoll ” a little south of the upper Indian village. No relics have been found in graves here. The former existence of “an Indian village on the flats” has been pretty generally known to Naples people, but it has never been an object of special attention or interest until recently the writer has undertaken to ascertain, as nearly as possible, the precise location of the two villages as shown by the distribution of the relics and to collect whatever might be found that bore clear evidence of having been fashioned or used by those who dwelt in them. When it is remembered that the inhabitants were not driven away from their homes hurriedly but had abundant time in which to remove whatever they considered of value; that the land has been under more or less vigorous cultivation by the whites for 120 years, and that less than % of the area can now be satisfactorily searched, the remaining 4/5 being covered by heavy turf, the quantity of the material collected, if not the quality, is of some interest. SIXTH REPORT OF THE DIRECTOR 1909 219 The material consists of stone mortars or anvils, pitted ham- mer stones, pestles, sinkers, hoes, celts, arrows and other flint articles, pottery in fragments and stems of pipes, etc. Mortars or anvils. These are blocks of gray sandstone from the local Portage flags, roughly dressed to a nearly circular shape 8 to 12 inches in diameter and about 2 inches thick, weighing 7 to 15 pounds. On one side a shallow cup-shaped depression has been picked out by hard blows with a sharp instrument, leaving a rough surface. The other side is usually slightly concave and smoothly polished, probably by use of a muller in pulverizing substances wemedtely. 21 Of these were found, 18 in the vicinity of the lower site, one at the upper, one hali a mile east of the lower site and one half a mile southwest. Many broken fragments occur. Hammer stones. These are mostly round or oval flattened drift pebbles from the nearby creek bed weighing 1 to 4 pounds. (wer 200 01 these were found, 145 at or near the lower site, 54 at the upper, one half a mile east and another half a mile southwest of the lower site; 33 of these show by the battered condition of their ends and sides that they have been used as veritable hammers against some hard substance, possibly to pulverize the rock mixed with clay in the process of manu- facturing pottery. 18 are granite or schist, the others being of hard quartzite or sandstone. The pits om these are large, shallow in proportion to size and worked smooth. The pits aid very much in getting a firm and easy grasp of the imple- ment. 4 are flat blocks of sandstone 1% to 2 inches thick and have a funnel-shaped pit on one side only an inch in diameter and % inch deep. The pit on one block shows that it was made by a rotary drill. The other specimens are all sandstone, mostly Portage or Medina, and in shape range from globular to irregu- larly angular. The pits also show a variety of shapes, some being large and worked out smoothly at the expense of con- siderable labor, the other extreme being those made by a half dozen hard blows with a sharp pick. 5 have two pits on one side. While the most of these pitted stones would be serviceable in cracking nuts, grinding corn and similar substances, some of them are not at all suitable and evidently were not designed for such use. Pestles. One 24% inches long, very roughly dressed. One 14 inches long, flattened and slightly curved; one 12 inches long, 1 % 220 NEW YORK STATE MUSEUM inches in diameter, very symmetrical and polished; one 6 inches long, very crude, and fragments of 9 others, were obtained. Sinkers. ‘These embrace 71 flat pebbles of sandstone 2 to 4 inches in diameter and 4 to 3% inches thick with two notches opposite each other on the edge. Hoes etc. 22 thin pieces of sandstone 3 to 6 inches across and % to 34 inches thick with the edges on one or more sides chipped thin, were found. Some of these were doubtless hoes, others may have served as axes. Pottery. Fragments of clay vessels: are very abundaneear the lower site where the subsoil is a fine plastic clay quite suitable for the potter’s use. 350 fragments I to 3 inches across and lz to % inch thick were collected, ali of which show surface ornamentation and 30 or more of them that of the rims. Pottery fragments are very rare at the upper site. Parts of. 9 pipe stems and of two bowls, one of the latter of stone, the others of clay, were found. Flints. Those found on the sites consist of 26 arrow points entire, 20 nearly so and 20 others much broken, or spoiled in making. Also 4 perforators or drills, all with points broken off. A small curved knife, a small gouge, and a quart of chips or flakes. These are very abundant. | The arrows are all small and triangular in shape. Except one, which is translucent white quartz, they are common dark to light chert, such as occurs in layers and nodules in the Onondaga lime- stone. The only flint article found on the sites that has a stem is one of the perforators, though many stemmed arrows and spears have been found on the higher ground south of the sites, specially _in the vicinity of a large spring near the railroad station in Naples and another half a mile south of the village. Besides the above named articles there were found 2 celts, 2 stone balls, 3 stone disks and a few others that show artificial shap- — ing for some unknown purposes. | Mortars, pitted stones, sinkers and flints similar to those above described were found on a small site near the West river bridge, 3 miles northeast from the village on the flats, where the first white settlers in 1797 found an Indian village composed of a few wigwams. Like that of all the New York Indian nations, the early history of the Senecas is buried under legends that, although apparently purely mythical, may be not only allegorical but traditional as well and containing germs of real history. SIXTH REPORT OF THE DIRECTOR 1909 221 The several versions of the legend concerning the origin of this nation all agree in locating this event in the region about the south -end of Canandaigua lake. To those who are acquainted with the topography of this region it would not be an overtax on credulity to believe that a band of Indians wishing or compelled to emigrate from their home on the Seneca river, and finding their way toward the west barred, possi- bly by hostile tribes, should take their course toward the southwest, through the West river valley and on arriving at this rich and spacious but sheltered and secluded intervale among the great hills, should actually make their first settlement and form their first village here. And it is entirely. reasonable to believe that, dwelling here in peace and plenty, their numbers would increase as the years passed, until having extended their occupancy down the lake shores and into the many warm valleys among the hills, the chief men among them should assemble on beautiful Genundewa, light their first council fire and bring into life a new nation with the significant and appropriate name Nun-da-wa-o-no, the People of the Great Hills. Rr gat 9, : : { ¥ ) ; j ke ay 3 ty } ; \ f f Ay ra oe , a J F F | i , | a 1 | F 1 y } ] : | UN DEX Accessions to collections, 76-96. Pidirendacks, 12-14; gold. sands, 29-32. mitxety, j., cited, 195. Albion quadrangle, 9. Allentown formation, 131. Alsen, 159, 160. Altered sandstone, 16. Amsterdam quadrangle, 20. Anorthosites, 14. Archeology, report, 59-69; bulletin, 74; additions to collections, 94- 95. Areal geology, 8-20. Arietta, 20. Arthursburg, Io. Asaphus, 136. Aspidocrinus, 158. Attica quadrangle, 9. Ausable lake, lower, 13. Avalanche lake, 13, 14. Barrell, cited, 150, 152. Basaltic dikes, 14. Bastatd granite, 16. Bastite, 17. Batavia quadrangle, 9. Batchellerville fault, 12. Beauchamp, mentioned, 214. Beckenkamp, cited, 202. Becraft limestone, 159. Beekmantown limestone, 11, 98, 99, mri, 120, 130, 131, 130. Benson, 20. Berkey, cited, 14. Biotite, 16. Birds, of New York, 58-59; oste- ology of, by R. W. Shufeldt, 73. Bison, 46. Black River limestone, 126. Bleecker, 20. 107, i114, Bleecker Center, 20, 21. Blister beetle, Say’s, 52. Blister mite, 49. Botts neporty 47-40, 735 Botany, bulletins, 73, 74; accessions to collections, 82-83. Bramendy-cited, 68," 102103, 05, 100. Biteiianad,) Ae PS citeds nm ae2O Broadalbin, 129. - Broadalbin quadrangle, 11, 20, 114. Brookite, 197. Brown tail moth, 51-52: Bulletins, published, ONGESSH Als 7G; -7As oti Calciferous of Champlain and Mo- hawk valley, 102. Calciferous sand rock, fossils, ror. Calcites, memoir on, 39. Caledonia quadrangle, 9. Cambrics and @zarkic: between, 132. Camillus formation, I50. Campbell, M. B., cited, 146. Canadian contact. with, ©zarkic and (Ordovicic,, 132: Carmelo 35: Cascade lakes, 13. Catskill, 159, 160. boundary Cattaraueus county;: rock’. cities) 25-20. Caves, joint caves of Valcour island, by G. H. Hudson, 161-96. Cementon, 160. Chadwick, George H., Downward Overthrust Fault at Saugerties, 157-60. Challenger report on deep sea de- posits, 152. Champlain, Lake, see Lake Cham: plain. 222 v 224 NEW YORK STATE MUSEUM Champlain’ valley, studyason y@al- ciferous formation, 102. Chazy limestone, 130, I61. Chionitey ao: Cigar case bearer; 49: Clark, B. W., mentioned, 9. Clark, Gov. Myron H., Museum of Iroquois ethnology, 64-69. Clark, N. W., mentioned, 216. Clarks Peck citeds mars. Clarke, Cora H., acknowledgments tonne: Clarke, J. M:) Early Devonic ot New York and Eastern North America, 70. Cleland) xcited,\102; 421165 onto mars: Clinton formation, 21-25. Clinton iron ores, 23. Clintonville, dikes, 23. Codling moth, 4o. Coeymans limestone, 157, 159. Cole? Thomas. 158156710 Color in the Vernon shale, origin of, by W. J. Miller, 150-56. Colummania,. 1177 Oe Conococheague formation, I3I. Contributions to mineralogy, by H. P. Whitlock, 197-203. Converse,) He ME Miytlis anal Legends of the New York State Iroquois, 74. Cranesville section of Little Falls dolomite, 116; T17~16) 120; Crinoidea, Devonic, monograph of, 43-45. Crush zones, 15. Cry ptozoon a12030122- 929 bese. proliferum, 98, IOI, I09. Steel, waz. Cumings, «i IR aciteds o2samiis: Cushing, H. P., survey of Saratoga quadrangle. 1: cited) slO2)127, 137. & Ulrich se Oe iece and Relations of the Little Falls Dolomite of the Mohawk Valley, 97-140. Dalmanella, 124. wemplei, I19, 136. Dana, cited, 143. Davis, cited, 160. Depew quadrangle, 9. Devonic of New York and Eastern North America, by J. M. Clarke, 70. Dictyonema flabelliforme, 134. Dikes, near Clintonville, 23. Dolomite, II. Earthquakes, record of, 35-39. Eccyliomphalus, 117. multiseptarius, 136. Economic geology, accessions to collections, 76-77. Eggleston, J. W., 160. Elizabethtown quadrangle, 12. Elk lake, 13. Elm leaf beetle, 50. Emmons, Ebenezer, cited, — 100; mentioned, 108. Entomologist, report, 48-54, 73. Entomology, bulletins, 72-73, 74; accessions to collections, 83-88. Eopaleozoic systems, 132. Epidote, 16. Esopus shale, 1509. Ethnology, report on, 61-69; addi- tions to collections, 95-96. Eurypterida, monograph of, 40-43. Fairchild, H. L., Glacial Waters in Central New York, 71; cited, 2m Faults, 12, 15,17} at «Sausemedase 157-60. Bavosites, 157. Feldspar, 16. Felt, E. P., Control of Household Insects, 72. Fishkill limestone, 18, 19. Fishkill mountains, 16, 17. Fishkill village, 16. Flat creek, 120. Fleming, cited; 155. Flies, 52. Fluorite, 198-99. ee PvE TOVSEXTH REPORT OF THE DIRECTOR 1909 Folklore, Iroquois, 63. Fonda quadrangle, 20. Fordham gneiss, I5. Forest insects, 50—-5I. Forest of Dean Mine, 35. Fort Montgomery, 35. Fossils, revision of Eopaleozoic systems, 134. Fruit tree pests, 48-40. Fucoidal beds, It. Fulton county, II, 20. Furnaceville ore, 23. Gabbro, 14. Gall midges, 52-53. Galway formation, 12. Gatnet, 14. Garoga, 20. Genesee shale, 23. Geneva-Ovid quadrangles, geology of, by D. Dana Luther, 72. Geological map of New York state, 8. Geological maps, 74; list, 8-9. Geological survey, report on, 8-47. Geology, areal, 8-20; surficial, 20- 21; special problems, 21-32; in- dustrial, 32-35; bulletins, 70-71, a7 4: Giant mountain, I2. . Glacial geology, 21. Glacial waters in central New Maree by H. L. Fairchild, 71. Glenham belt, 16, 17. . Glens Falls, 114. Gloversville quadrangle, 20. Gneissoid type, 16. Gold sands of the Adirondacks, 29- a2) Goldschmidt, V., cited, 201, 202. Gordon, C. H., cited, 16. Granite, ITI. Grano-diorite, 15. Grape blossom midge, 4¢—-50. Grape root worm, 50. Greenfield limestone, go. Grenville rocks, 11, 13, 16. Gypsum, 32-34, 201-2. Gypsy moth, 51-52. 225 Hall, James: cited? 22: 25; 10r. Hamilton shale, 24. Hartman, Panny “Pa works On. 53; 54. Hartnagel,.C. A., mentioned, 197. Haug, Emile, cited, 143. Herkimer county, 20. Hickory bark borer, 51. Puehland Park, section» of Wittle Falls dolomite, 107, 108-14. Highlands, geology of, 14-20. Homalonotus vanuxemi, 159. Honeoye quadrangle, 9. Hornblende, 16, 17. Hortontown, 17. House fly, 52. : Household insects, control of, 53, 72, Howard, L. O., acknowledgments to, 54. Hoyt limestone, If, 90, 101, 103, 105, TO7Ze TL, ELS, / Wie aon Ou aa. Hoyt quarry, 109. Hudson, George H., Joint Caves of Valcour Usland, 101-06: Hudson highlands, geology of, 14- 20. Hudson River slate formation, 10. Hyolithellus micans, 17. Indians, report on, 59-69. See also Iroquois. Industrial geology, 32-35. Inwood limestone, I5. Iron ore explorations, 35. Iron oxids, 16. Irondequoit limestone, 23. Iroquois, myths and legends, by hese Converse, .74. Iroquois and the struggle for America, by Elihu Root, 204-12. ethnology, 61-69; Gov. Clark Museum of, Troquois Myron H. 64-69. Ithaca, igneous rocks, 23. Ithaca shales, 23. Jefferson county, section, 102. 226 Joint caves of Valcour island, by G. H. Hudson, 161-96. Jordan sandstone, 132. Julien, cited, 150. Kalkberg limestone, 159. Keene valley, 13. Kemp, J. F., cited, 12; mentioned, 199Q. Kirk, cited, 43. Labradorite, 14. Ladue, Ward, mentioned, 17. Lake Champlain, solvent power on its limestones, 173-83. See also Valcour island. Lake Sanford region, 35. Lassellsville quadrangle, 21. Leighton, Henry, mentioned, 201. Leptaena rhomboidalis, 158. Leptocoelia, 158. flabellites, 158. Leray limestone, 126. Linden moth, snow-white, 51. Lindsley Corners, 20. Lingulepis acuminata, IOI, 104, 107, TOM Mol. ar Oe oats pinniformis, 18. Little Falls dolomite, 11, 12; of the Mohawk valley, age and rela- tions, by E..O. Ulrich and 1. P- Cushing, 97-140; does not prop- erly belong with the Beekman- town, 103; Ticonderoga section, TOR esr Saratoga Section, 100-14; Whitehall section, 114-16; Mo- hawk. valleys Sections, UG.20; western sections, 120-27; Little Falls section, (116, 120-24). 120: correlation of foregoing sections, 128-30; chart of sections, 129; stratigraphic position, 130-36. Lockport quadrangle, 9. Lowville limestone, I13, II4, 117, ILO, 12%, 124) 12ey eae Oe a Ludlowville, igneous rocks, 23. Luedecke, O., cited, 201. Luther, D. D., resurvey of certain quadrangles by, 9; additions to NEW YORK STATE MUSEUM archeology section, 60; study of ancient Indian settlements, 69; Geology of the Geneva-Ovid Quadrangles, 72; Nun-da-wa-o, the Oldest Seneca Village, 213-21. Magnetite, 17, 35, 199-201. Manhattan island, geological struc- tures, 14-16. Manheim dike, 23. Map, geological, state, 8. Maps, geological, 74; list, 8-9. Mastodons, 45-47. Mather, W. W., cited, 16. Matteawan, 16, 17. Matteawan granite, 16. Maw, cited, 150, 155. Mayfield, 20. Medina quadrangle, 9. Melilite, 24. Memoirs, published, 70; in press; 74. Micaceous gneisses, 16. Microcline, 16. Middle Stink lake, at. Middleville section of Little Falls dolomite, 116, 124-20)9120. Miller, Hugh, cited, 155. Miller, W. J., survey ormbroade albin quadrangle; 11) Geology, of the Remsen Quadrangle, 70; of New York work of, 114; Origin of "Coloma in the Vernon Shalem nsea,508 Clhed UTS Mineralogy, 39-40; accessions to collections, 79-82; contributions to, by H. P. Whitlock mo7-2a¢ . Mines and quarries, review of, 34- 35: Mining and quarry industry of New York, by D. H. Newland, a1, Mohawk valley, Little Falls dolo- mite, age and relations, Samy BE. O. Ulrich and Hy PY Casha 97-140; sections of Little Falls dolomite, 116-20; surficial geol- ogy, 20. INDEX TO SIXTH REPORT OF THE DIRECTOR IQCQ 22 Mohawkian limestone, 120. Mollusca, monograph of, 56. Moose, 406. Morgan, Lewis H., cited, 214. Mt McIntyre, 12. Mit Marcy, 12, 13: Mt Marcy quadrangle, I2. E25. -0D, New Scotland beds, 158, 1509. New York, southeastern, geology wba. Newark sandstones, ISI. Neweand, DD. H., Mining and Quarry Industry of New York, 7X. Newport section of Little Falls dolomite, 116, 126-27, 120. Niagara formation, I50. Northville, 21. — Nun-da-wa-o, the oldest Seneca mies. by ©. 1: Luther, 213-21. Obolella, 18. Olean conglomerate, 27. Olean Rock City, 27. Olenellus sp., 18. Oneota dolomite, 132. Ophileta, tot. _disjuncta, 117. levata, I21. Ordovicic, contact with Canadian and Ozarkic, 132. Oriskany beds, 158, 159. Orthoclase, 16. Oscillations of level, 137-40. Ozarkic and Cambric, boundary between, 132. Paleontology, 40-45; bulletin, 72; accessions to collections, 77~78. Paleozoic platform oof North America, symmetric arrange- ment in the elements of, by Rudolf Ruedemann, 141-49. Pamelia formation, 102. Parrish, quoted, 216. Pearls, investigation of rences, 56-58. OCcur= | Phelps quadrangle, 9. Phytopsis,- 1245, 127. Pinnacle, 21. Pinnacle mountain, 20. Pitchoff mountain, 14. Plagioclase, 16. Plant lice, 48. Plectambonites sericeus, 19. Pleistocene deposits, 12. Pleurotomaria hunterensis, 121, 128. Port Ewen, 158, 150. Port Henry quardrangle, 12. Portage shales, 23. Postglacial mammalian remains, 45-47. Potsdam sandstone; 11, 12) 18, 08, OOr 4 LOS LOZ Lies DIAN ATIC. TiS, 120, 120;4130, 138, 130;- fossils, IoI; stratigraphic position, 130- 30. Pore tenbee cited. 27, Poughkeepsie quadrangle, 16. Prasopona simuulattiney bi4,. 12% T24: Prosser: ©.) S,, .cited, 102.4, 116; ITO, 120. Protean group, 22. Publications, 69-74. Pyrites, 35. Pyroxene, 147 17, Quartz, 106. Quartzite, 17. Remsen quadrangle, geology ot, by W. J. Miller, 7o. Ribeiria, 119, 136. Rochester shale, 22. Rock cities of Cattaraugus county, 25-20. Rock City- Falls, 113, 114. Rock hollow, 17. Rondout, 159, 160. Root, Elihu, The Iroquois and the Struggle for America, 204-12. Ruedemann, Rudolf, survey of Saratoga quadrangle, 11; Sym- metric Arrangement in the Ele- ments of the Paleozoic Platform 228 of North America, 141-49; cited, 12, 97. Russell, cited, 150, 151. Sacandaga valley, 21. St Lawrence limestone, 132. Salina beds, 23. San José scale, 49. Sangerfield quadrangle, 9. Saratoga county, ITI. Saratoga quadrangle, I1. Saratoga section of Little Falls dolomite, 98, 106-14, 129. Saratoga Springs, protection fer mineral water springs, 9-II. Saratogan series, 130-36. Saugerties, downward overthrust fault, by G. Ho Chadwick 157,00: Saunders, vAn ie) citeds ang lee nisce Schneider, P. F., investigation of pearls, 58. Schoharie grit, 158. Schuchert, Charles, cited, 135, 144, 147, 148. Scientific collections, condition of, 6-8. Scott, cited, 153. Sedgwick, cited, 132. Seely, cited, 98, 102, 103, 105, 106. Seismological station, 35-30. Shade tree pests, 50. Shaler, cited, 123. Shoreham, 103. Shufeldt, R. W., Osteology of IBhieelsy, 7/5 Sieberella galeata, 157. Skene mountain, section of Little Falls dolomite, 114, 115-16. Small Creek, section of Little Falls dolomite, 121-24. Smith, Burnett, cited, 23. sinyth Cas jen 2A: Sodus shale, 23. Solenopora compacta, 20, I'T7. Spirifer cyclopterus, 158. macropleura, 158. murchisoni, 158. Sprakers, 120, 120. Spruce bud worm, 51. NEW YORK STATE MUSEUM Spruce gall aphid, 50. Staff of the Science Division and State Museum, 75-76. Stissing mountain, 137. Stoneco, 18. Storm King, 15. Streptelasma, 126. Suess, cited, 141, 145. Sugar maple borer, 50. Surficial geology, 20-21. Sutton, S: Hig actted: 216: Swartoutville, 19. Syenite, II, IA. Syracuse, igneous rocks, 23. Taonurus caudagalli, 158. Tetradium, 117. cellulosum, 124, 127. Tetragraptus zones, 134. Theresa formation, 99, Iot, 127-28, 120, 130, 131, 130: Ticonderoga section of Little Faiis dolomite, 98, 103-6, 129. Titaniferous ores, I4. Topographic quadrangles, 8. Trenton limestone, 107, 121, 126. Tribes Hill limestone, 11, 99, tor, 113, II4, 117, 118, (20,5022 124, 126, 128, 134, 139, 140; strati- graphic position, 130-36; age of, 136-37. Tribes Hill section of Little Falls dolomite, 116, 118-19, 120. 102, 124, Ulrich, E. O.,. cited; 130) 13%, en MGA TAD as 7 & Cushing, H. P., Age and Relations of the. Wittle rails Dolomite of the Mohawk Valley, 97-140. Utica quadrangle, 9. Valcour island, joint caves of, by Gare saudson, 161-6. van Ingen, cited, 157. Vanuxem, cited, 22, 97, 100, 116, 154. INDEX TO SIXTH REPORT OF THE DIRECTOR IQOQ Vernon shale, origin of color in, by W. J. Miller, 150-56. Vly mountain, 16, 17. Walcott, cited, 99, 101, 116, 130, 134, 148. Wappinger Falls, 16. Wappinger limestone, 18. Watertown limestone, II3 II4. Wayland quadrangle, 9. Weller, cited, 141. Wheelerville, 2r. Whiteface, I2. Whitehall section of Little Falls dolomite, 98, 114-16, 120. 229 Whitlock, EH. P, (Contributions. to Mineralogy, 197-203; cited, 4o. Whitnall, H. O., work of, 9. Walhamss Hi./S: cited,.123: Williamson shale, 23. Willis, Bailey, cited, 141, 145, 147. Wolcott limestone, 23. Wolcottville, 16. Woodworth, J. B., cited, 195. Young, D. B., work of, 53, 54. Zoology, report on, 54-59; bul- letins, 73; accessions to collec- tions, 89-94. ha =) eee ee eee lo « 7 4 a oe ihe Ad Te we ri. Saeae A ier Ab \ ' Appendix 1 Geology — Museum Bulletins 135, 137, 138 y of the Port Leyden Quadrangle, Lewis (County, N.Y. af Education Department Bulletin Published fortnightly by the University of the State of New York Entered as second-class matter June 24, 1908, at the Post Office at Albany, N. Y., under the act of July 16, 1894 No. 463 PU BNI SONGS Y. JANUARY I5, 1910 New York State Museum Joun M. CrarkeE, Director Museum bulletin 135 GEOLOGY OF THE PORT LEYDEN | QUADRANGLE, LEWIS COUNTY, N. Y. BY W. J. MILLER PAGE PAGE MMGOMTGEHO IS = oi ois ws 3s eke 5 | baleozoresoveriap... Sheed Nee a7. General geologic features........ 6 | Surface of the Precambric rocks.. 39 Wopoesraphy and drainage:...... 8 | Pleistocene (glacial) geology.... 44 Precambric FOCKS/..5...%.65.... Op MES VEKOSiOjals Sacre ee ahr ae ee 46 leeware TOCKS. 2... ks ce os ZT ECOUOMIC PROGMNEES: 6 wok caies «. cs 56 minmisitifa @eOloey. .. J. .ecs... Gay nif ISOC kee mic Geo Poa ee 59 New York State Education Department Science Division, September 24, 1909 Hon. Andrew S. Draper LL.D. Commissioner of Education Str: I have the honor to transmit herewith for publication as a bulletin of the State Museum, the manuscript of a report on the Geology of the Port Leyden Quadrangle, Lewis county, prepared Dy Prof. W. J. Miller, a member of the staff of this division. Very respectfully Joun M. CLARKE Director State of New York Education Department COMMISSIONER’S ROOM Approved for publication this 24th day of September 1909 Commissioner of Education : : < i el » we ; feu * > ? = Be ees i i ° n = Ke \ ie t . 2 j > ‘ f e) te J fe ;, cv ioe N ~ } . le i xv a ¥ ‘ 4) C.. a Z / <7 Ns 4 2 J ts 5 © (Pina poe v= ie Education Department Bulletin Published fortnightly by the University of the State of New York Entered as second-class matter June 24, 1908, at the Post Office at Albany, N. Y., under the act of July 16, 1894 No. 463 ALBANY, N.Y. JANUARY 15, I9I0 New York State Museum Joun M. Crarkg, Director Museum Bulletin 135 GEOLOGY OF THE PORT LEYDEN QUADRANGLE, LEWIS COUNTY, N. Y. BY W. J. MILLER INDRODUCTION The Port Leyden, New York, quadrangle of the United States Geological Survey comprises the region lying along the western border of the Adirondack mountains and is included between latitude lines 43° 30’ and 43° 45’ north and between longitude Mieeeys 965 aud 75° 30’ west. The map covers 1/16 square degree or about 215 square miles of territory, all of which lies in Lewis county except a few square miles extending into Oneida county at the extreme southeast. The Rome, Watertown and Ogdensburg Division of the New York Central Railroad tra- verses the region from north to south through the Black river valley. Port Leyden, Lyons Falls, Glenfield, Martinsburg, Turin and Constableville are the principal villages. This region, like most others along the border of the Adiron- dacks, was at one time a dense forest which has nearly all been cut away, leaving only small wooded areas of second growth. Next to agriculture, the chief industry is the manu- facture of wood pulp and paper, the largest mills being located at Lyons Falls, Goulds) Mill, Kosterville, Shuetown, Lyonsdale and Port Leyden. The logs used are driven down Moose river. A number of small sawmills are still in operation. On the east side of Black river the soil is nearly always sandy and rather unproductive, while on the west side of the river the soil is usually rich and supports a prosperous farming com- munity. The principal products are milk and cheese. 6 Re ee NEW YORK STATE MUSEUM GENERAL GEOLOGIC FEATURES Under this heading it is proposed to briefly outline the geologic history of the whole Adirondack region so that the detailed study presented in this report may be made more in- telligible to the reader. This outline is based largely upon the admirable treatises of Prof. H. P. Cushing. So far as known the oldest rocks of the Adirondacks are those of Grenville (Precambric) age. They are sedimentary rocks, originally shales, sandstones and limestones, which have been highly metamorphosed into gneisses and crystalline limestone. These rocks are of unknown but great thickness, and are widely scattered throughout the Adirondacks, thus showing that the whole region was under water at the time of their deposition. After the deposition of the Grenville sediments the region was raised above the ocean level and the rocks began to decom- pose and suffer erosion. Either just before, during, or after the uplift, great masses of igneous rocks were intruded. The Gren- ville rocks were for the most part engulfed by the intrusion so that only occasional patches of them were left intact. After the igneous activity the rocks became thoroughly meta- morphosed by being squeezed, highly folded and converted into eneisses. Such changes can take place only at great depths (several thousand feet) and hence we are led to the belief that a vast erosion of the original land masses must have taken place. This in turn signifies that the land masses must have remained above sea level for an immense length of time. At or toward the close of this long period of erosion, igneous activity of a minor character took place. The basic igneous rocks erupted at this time are especially well shown in the northeastern Adirondacks, where they were squeezed up between joint planes in the older rocks. That these rocks are much younger than the igneous rocks first mentioned is clearly shown by their mode of occurrence and their general lack of metamorphism. Toward the close of the erosion period the region of the Adirondacks was nearer the sea level and of slighter relief than at present. Then the whole region began to sink slowly, allow- ing the sea to encroach upon the land until only an island was left or probably even until the whole region was under water. During the subsidence, deposition of Paleozoic sediments went GEOLOGY OF THE PORT LEYDEN QUADRANGLE 7 on, one layer above another, the younger deposits overlapping each other and encroaching upon the sinking land surface. Since the subsidence was not entirely uniform on all sides certain local variations in deposition occurred. The first of the deposits to form upon the sinking floor was the Potsdam (Cambric) sandstone now found exposed nearly everywhere except along the southwest border. After this the sediments changed in character and the limestones of the Beek- mantown (Lower Siluric) were laid down. Then followed the deposition of the highly fossiliferous Trenton (Lower Siluric) limestones including the Lowville and the Black River lime- stones. The fairly clear waters full of animal life then gave way to the muddy waters of the Utica, when the Utica shales (Lower Siluric) were deposited. At this time the Adirondack region was probably all under water. Next came an uplift on the east and northeast where depositions ceased. On the south and southwest, however, deposition continued and the successive formations of the Siluric and Devonic above the Utica shale were laid down. These Paleozoic formations may now be seen as ene passes from the Adirondacks southward to the southern border of the State. The last period of igneous activity in the Adirondacks occurred some time after the close of the Lower Siluric. This activity was of minor extent and showed itself in the form of dikes. At some time after the deposition of the Utica shale the rocks, especially along the southern border, were deformed chiefly by faulting. A series of these faults extends across the Mohawk valley. The western Adirondacks, including the Port Leyden quadrangle, have been subjected to erosion for a vast length of time, certainly since the close of the Paleozoic and more than likely since the Devonic. During this great lapse of time a large amount of material has been removed. Doubtless the whole Port Leyden quadrangle was at one time covered by the Utica and Lorraine shales, which have all been removed except along the western side. The superficial deposits, such as the sands and gravels which are so prominent in the Port Leyden district, were tormed by, or along the border of, the great ice sheet of the Glacial age.. From the geological standpoint this ice sheet was present only quite recently and covered most of New York State. 8 NEW YORK STATE MUSEUM TOPOGRAPHY AND DRAINAGE The Black river valley may be looked upon as the principal topographic feature along the western border of the Adiron- dacks, and the Port Leyden quadrangle represents a consider- able portion of this! valley where it is deepest. Blackiaives enters the quadrangle at the southeast corner at an elevation of tooo feet and, after following a northwest-north course, leaves it near the middle of the northern boundary at an elevation of about 740 feet. From the river eastward there is a general upward slope toward the Adirondacks. Facing the river there is a steep slope, which within 2% miles, passing eastward, gives way to a generally level sand-flat area lying at an elevation of from 1200 to 1300. Along the eastern edge of the map several points reach altitudes of from 1300 to 1340 feet. Passing westward from the river the general rise is much more rapid. Two terraces are here well developed from the latitude of Port Leyden northward. The lowermost terrace is from 2% to 4 miles wide and has a steep front rising from 300 to 400 feet just west of the river. The uppemiter race is known as Tug hill whose very steep eastern front rises from 400 to 450 feet and makes up the western por- tion of the quadrangle. The highest point on this side of the river is Gomery hull, mear the western edge of themmap which shows an elevation of nearly 2100 feet, while altitudes of 1800 to 1900 feet are common. ‘This high ground to the west of the river is a part of the broad high land area which lies between Black river and Lake Ontario. It is interesting to note that the elevations of the western portion of the quadrangle are much greater than those of the eastern or Adirondack portion. In order to reach elevations of 2100 feet or over it is necessary to pass 20 or 25 miles east of Black river into the Adirondacks to the high points around the Fulton chain of lakes. Within the map limits Black river descends 200 feet, theaaen a series of still waters and rapids, before reaching Lyons Falls. At Lyons Falls there is a sudden drop of 60 feet, but from this point northward to the map limit the river flows by a winding course through an old lake bottom [see p. 54] and the gradient is almost imperceptible. The largest tributaries to Black river from the east are Fall brook, Moose river, Fish creek, Otter creek and Independence river. By far the largest of these is Moose _ OE —————— GEOLOGY OF THE PORT LEYDEN QUADRANGLE 9 river, one branch of which drains the Fulton chain of lakes. Chief among the tributaries from the west are Sugar river, Mill creek, House creek, Whetstone creek and Roaring brook. All the larger streams which have cut across the steep eastern front of Tug hill have there cut out deep narrow gorges locally called “gulfis.” More special physiographic features will be described later. Pim CAV RIC ROCKS The Precambric rocks of the quadrangle represent a portion of the great Adirondack crystalline mass along its extreme west- ern border. They occupy the eastern side of the quadrangle and mesma wittle less than one half its area. Except at the extreme south the Paleozoic-Precambric boundary line is every- where to the west of Black river, but it keeps close to the river bottom. These crystalline rocks continue westward, under cover of the Paleozoics, for many miles. Considerable portions of the Precambric area are so deeply buried under glacial drift deposits that it is impossible to gain even the slightest clue as fovtm@evecharacter of the rocks in those places. Grenville gneiss The Grenville formation takes its name from Grenville, Canada. It comprises a series of gneisses representing very ancient sedimentary rocks which have been so profoundly meta- morphosed that the original sedimentary features have been largely obliterated. So far as can be definitely proved they are the oldest exposed rocks in the whole Adirondack region. That they are not actually the oldest rocks is evident from the fact that these sediments must have been deposited upon a still older floor. This very ancient rock floor, which may or may not represent a portion of the earth’s primitive crust, has thus far not been proved to exist in the present exposures of the Adiron- dacks. It is barely possible that some of the gneisses still of doubtful age and origin may represent that ancient sea-floor. Within the map limits the Grenville has been mapped in only three small areas, one at Kosterville, another at Lyonsdale, and a third to the east of Fowlersville. Grenville rocks are unques- tionably present in much greater force than these small areas seem to indicate but they are always so thoroughly .involved with other gneisses that they can not be represented on the geo- IO NEW YORK STATE MUSEUM iogic map as such. Occurrences of this kind will be described later. One of the strongest proofs of the sedimentary origin of the Grenville is the presence of limestone beds in the formation. Such limestones have been described by Smyth! in the Diana- Pitcairn area some 30 miles northward and also at the Ful- ton chain-of lakes some 25 miles eastward. A little has been found by Mr D. Hi. Newland in the Little Falls districiyanmd also on Moose river a few miles east of the Port Leyden quad- rangle. The latter occurrence is the closest to the Port evden quadrangle so far known. The writer has found no actual lime- stone on either the Remsen or the Port Leyden sheet although certain gneisses usually associated with the limestone are pres- ent. The statement may be repeated that, whereas Grenville limestone is common along the northwestern Adirondacks, it is only sparingly represented along the southwestern border. The fact that commonly the Grenville rocks here amd else- where are in alternating layers which stand out in sharp con- trast because of marked differences in composition and color leads to the belief that these bands are due to differences in original sedimentation. At times the gneiss is composed of almost pure quartz and could scarcely be of igneous origin. Graphite is a form of crystallized carbon and of organic origin. Its presence as flakes in certain of the Grenville gneisses, in- cluding some within this quadrangle, affords a strong argument in favor of the sedimentary origin of those gneisses. Garnet is frequently present, often in great abundance, and it is rather more common in metamorphosed sediments. Of the three areas above mentioned, each has certain dis- tinctive features and hence they will be separately described. Thus in the Kosterville area the rocks are mostly quartz-silli- manite gneisses in thin layers and weathering to a rusty brown. They are not sharply separated from the neighboring rocks and some feldspar-garnet gneisses appear near the northern border of the area and along the river below Shuetown. The dip of the foliation is northward while the strike is about n. 60° e. which is the same as for the surrounding rocks. The specimens here described were taken from the fine exposures just below the bridge across Moose river. Microscopic study shows one 1 Crystalline Rocks of the Western Adirondack Region. N. Y. State Mus. 51st AnvRep’t. 1807. 927460-07, Plate 1 Grenville gneiss just below the Moose river bridge at Goulds Mill. The rock is here practically a thin bedded quartzite. GEOLOGY OF THE PORT LEYDEN QUADRANGLE eT specimen to be made up as follows: quartz 75%; sillimanite 124; and with the long axes of the glistening needles parallel to the rock bands; enstatite 54; magnetite 3%, and changing to leucox- ene; pyrite 2%; garnet 2%, and often completely enveloping the magnetite; together with a little zircon and badly decomposed biotite. Another specimen shows from 85 to 90% of badly cracked quartz; 1 or 2% each of hornblende, pyrite and sillimanite with a little zircon; while the rest of the rock is made up of gray, uncrystallized, yellow-stained, decomposition products of horn- blende and biotite. Certain other layers are slightly feldspathic. The most striking features in the composition are the very high quartz content, the almost complete absence of feldspar, and the dearth of dark colored minerals. The rock thus appears to have been an almost pure sandstone which has been meta- morphosed to a quartzite. The rock is highly cataclastic and that the mass has been subjected to a great pressure is proved by the local folds and by the general crushed appearance of the exposures [see pl. 1]. In the field the rock has a decidedly sedi- mentary look and we have here a fine example of the Grenville which does not appear to have been very profoundly changed from the original sediment. Where these gneisses grade into the surrounding mixed gneisses some feldspar and a larger per- centage of dark colored minerals are present. The Grenville rocks in the Lyonsdale area are chiefly feldspar- garnet-mica gneisses. The gneissic structure is here greatly accentuated by the alternation of light and very dark gray layers which are usually from a few inches to a foot or more in thick- ness. A thin section of the light gneiss shows quartz 754; feld- spar 15 to 18%, mostly oligoclase to labradorite, but with a little microperthite; biotite 5%, and garnet 2 or 3%. In the dark gneisses the quartz is proportionately less prominent while the biotite may run as high as 35 or 40%. Both the light and dark rocks are often very garnetiferous. In some specimens a few small flakes of graphite were noted. The original sediments here were probably somewhat carbonaceous shales and shaly sandstones. The rock bands show a northward dip at a high angle and a strike of n. 40° e. On the north side the exposures are not good but the Grenville does not seem to be sharply separated from the surrounding rocks, while on the south side, along Moose river, there is exhibited a very sharp contact between the Gren- I2 NEW YORK STATE MUSEUM ville and the syenite. The more resistant syenite here forms a high, steep rock-wall on the south side of the river, while the less resistant Grenville gneisses have been deeply trenched by the river [see pl. 2]. Moose river really bears about n. 40° e. here and parallel to the foliation instead of nearly east and west as shown on the map. In the area east of Fowlersville the Grenville rocks are chiefly pyroxene gneisses. The gneissic structure is highly developed and accentuated by the alternations of light and dark colored bands although none of the rocks are very dark colored. The bands are seldom more than a few inches thick. Microscopic investigation shows the common rock to be made up as follows: 40 to 50% of quartz; 25 to 30% of large, bright green, pyroxene crystals, sometimes slightly pleochroic; about 25% of feldspar, mostly orthoclase together with a little acid plagioclase; 3 to 54 each of hypersthene and enstatite; and a little bronzite and white pyroxene. Judging by the composition the sediments from which these rocks were derived were probably shales or shaly sandstones possibly somewhat calcareous. These gneisses are very similar to those referred to by Smyth as being directly associated with limestone. Although no limestone is here seen in outcrop, it is possible that some does occur along the east side of the area which may thus account for the distinct depres- sion (now drift-filled) along that side and from which some softer or less resistant material has certainly been removed by erosion. Associated with these gneisses are a few layers rich in basic plagioclase feldspar and poor in pyroxenes and which have the appearance of igneous rocks. This Grenville area forms a long, narrow ridge which stands out as a distinct topographic feature. Moose river has cut a channel across this ridge. The rocks dip at an angle of 40° or 50° westward and strike almost due north and south. Outcrops of syenite have been found on all sides of, and pretty close to the Grenville mass. There are no sharp contacts visible but it seems certain that we are here dealing with a long, narrow inclusion of the Grenville in the syenite. This matter will be further discussed below under the heading “ Syenite gneiss.” Syenite gneiss As indicated on the geologic map, syenite gneiss makes up a considerable portion of the known Precambric area. From the standpoint of both composition and structure it is very uniform ee Se ee Te ek eee ee a Re - Dieyy Plate 2 Wiel Miller, photo Moose river gorge just east of Lyonsdale. The rocks in the bed of the river are garnetiferous gneisses belonging to the Grenville. The high, steep rock on the right side is syenite which is in sharp contact with the Grenville. GEOLOGY OF THE PORT LEYDEN QUADRANGLE 13 over pretty large areas and it is clearly the most homogeneous rock mass among the Precambrics. The typical rock is a quartz- hornblende syenite always showing the granitoid texture. The quartz content varies a good deal but apparently without other- wise affecting the rock. The dark colored minerals are always very subordinate in amount. On weathered surfaces the color of the rock varies from a light brown to a reddish brown, while the color of the fresh rock varies from a sort of greenish gray to a light gray. The rock is nearly always medium grained although somewhat variable in this respect. In the field the rock always clearly exhibits a gneissic structure which usually can not be made out in the hand specimen. A distinct banding is seldom shown except at times near the borders where the syenite grades into the surrounding rocks. The minerals are roughly arranged with their long axes parallel to the strike of Dieetatomowiich tanges from n. 30° to 70° e,. Such an arrangement of the dark colored minerals causes the foliation to be more evident, but they appear like wavy streaks which are seldom continuous for more than a few inches or a foot. The homogeneity of this syenite and its lack of distinct banding Serve to Separate it from the other Precambric rocks in the field. The only noteworthy departure from homogeneity is to be found in the presence of occasional small dark basic patches in the syenite. These fpatches nearly always show abrupt termi- nations and to all appearances they are true inclusions. They are rich in hornblende and biotite and are invariably arranged with their long axes parallel to the gneissic bands of the syenite. Such inclusions may be seen in the field southeast of Denley; near where Miller brook enters the quadrangle; and probably best in the large exposures southwest of Partridgeville. Most of the syenite outcrops are, however, entirely free from such inclusions. A number of syenite areas are shown on the accompanying geologic map. Of these the southernmost one extends from Denley southeastward to Hawkinsville and represents probably the purest and most typical syenite of the region. Fine expos- ures occur in the fields southeast of Denley and in the vicinity of Hawkinsville. A large area extends from Miller brook north- ward to Moose river with good outcrops along Fall and Miller brooks; at Fowlersville and for 2 miles southward; and just east of Lyonsdale. Another large area occupies the northeastern I4 NEW YORK STATE MUSEUM portion of the quadrangle with fine exposures between Brant- ingham lake and Partridgeville and also where the road leaves the map east of Brantingham post office. The area between Greig and Donnattsburg shows many large outcrops of rock which here as well as around Partridgeville are more quartzose than usual. Smaller patches of rather quartzose syenite are shown at Lyons Falls and in the river bottom east of Glenfield. The rock exposed in the quarry southeast of Denley may be taken as typical of the best syenite of the quadrangle and a detailed description of this type will now be given. In thin section fresh feldspar is seen to be the most common minerai which makes up 75 to 80% of the rock. Much of the feldspar ig present as microperthite usually in large crystals and with the microperthitic structure beautifully exhibited. There is also a considerable percentage of another feldspar, presumably anor- thoclase, which is characterized by a sort of moire or clouded appearance. There is a small amount of plagioclase feldspar ranging from oligoclase to andesin. The second most common mineral is quartz of which there is 12 or 15%. The quartz grains are very variable in shape and size and are frequently broken as a result of pressure. Of the dark colored minerals hornblende and biotite make up about 5% of the rock. The hornblende is the common green variety with usual pleochroism and shows frequent alterations to chlorite. I or 2% of magnetite, some- times with leucoxene borders, is also present. Beside these a few small crystals of zircon, apatite, and zoisite may be seen nearly always ‘as inclusions. A study of the thin sections from the different syenite locali- ties shows a range of minerals as follows: Feldspar 60 to 80% —ymicroperthite always abundant, anorthoclase none to 20%, oligoclase none to 10%; quartz 15 to 30%; hornblende none to 54; biotite none to 3%; magnetite none to 3%, and zircon, apatite and zoisite are nearly always present in very small amounts. In one or two cases a little garnet has been noted. The cataclastic structure is always more or less well developed in the syenite, sometimes being very prominent, which shows that the rock must have been subjected to a pretty severe dynamic meta- morphism. : In Cushing’s! typical syenite at Loon lake and Smyth’s® typi- " 1Geol. Soc. Am. Bul. 1899. 10:177-02. 2 loc. cit. p. 473. GEOLOGY OF THE PORT LEYDEN QUADRANGLE 15 cal rock in the Diana-Pitcairn area, the dark minerals, especially pyroxene, are prominent constituents, while in the Port Leyden district the pyroxene is always absent and the dark minerals never amount to more than 7 or 8¢. Otherwise the rocks are very similar. In passing northwestward from Little Falls to Port Leyden the syenite loses its pyroxene and the microperthite becomes more prominent than the anorthoclase. It is now well established, especially by the excellent work of Smyth,! that the syenite is a plutonic igneous rock which has been intruded into and is therefore younger than the Grenville. The evidences from the Port Leyden region are clearly in har- mony with this view. Thus the Grenville area east of Fowlers- ville is surrounded by pure syenite and the writer is convinced that we have here a good example of a large Grenville inclusion in the syenite. Significant in this connection is the fact that the strike of the foliation in the Grenville is north and south while that of the nearby syenite is about n. 30° e. This would be expected especially where large sedimentary masses were caught up in the molten syenite. Near Lyonsdale, on the south side of the river, the syenite and Grenville are in sharp contact while north of the river they appear to blend into each other. Around Kosterville no sharp contacts are seen but the syenite and Grenville seem to be mixed around the borders of the Gren- ville. Referring to similar phenomena farther northward Smyth? says: “Some of these inclusions are clearly defined with sharp boundaries but others are somewhat blended with the surround- ing syenite as though they had undergone a partial melting.” The small basic inclusions above mentioned and the very inti- mate mixture of syenite and Grenville on a large scale as de- scribed below also argue for the intrusive character of the syenite. Granitic syenite gneiss In the northern portion of the quadrangle, and on either side of Black river, two areas of granitic syenite gneiss are shown on the geologic map. These areas are probably continuous under the broad drift-filled valley bottom. This rock is almost certainly a granitic phase of the normal syenite above described, and, since the one rock grades into the other, the drawing of a boundary line must of necessity be an arbitrary matter. In ~ 11oc, cit. atOC. til. D477, \ 16 NEW YORK STATE MUSEUM order to distinguish the gnanitic syenite from the normal syenite several features, given in the following description, must be considered. The rock is not only clearly gneissoid but also distinetly banded. The rock bands are straight and rather persistent and the minerals are commonly arranged with their long axes paral- lel to the foliation. Frequently the “leaf eneiss” effect is beau- tifully shown because of the flattening out of the quartz and feldspar crystais. The color of the typical rock is red although at times gray bands are present. The size of the grain is rather variable but mostly pretty coarse. At times the quartz and feldspar crystals are almost porphyritic. The average quartz content is noticeably higher than in the normal syenite and com- monly the more weathered surfaces show numerous projecting quartz crystals; often the rock might well “be called Mewamsre: The granitic syenite also lacks the homogeneity of the ordinary syenite. In the larger exposures of the typical red quartzose gneisses there are occasional bands of gray, less quartzose eneisses very similar to the normal syenite. 3 Another noteworthy feature is the presence of long, narrow patches or inclusions much like those sparingly present in the ordinary syenite, but they are here much larger and more numer- ous. They are always drawn out perfectly parallel to the folia- tion planes but they are seldom more than. 30 or 40 feet in length. They are composed of about equal parts of badly de- composed basic plagioclase and brown hornblende with which are associated thin layers of almost pure biotite. These biotite layers often give the rock a decidedly schistose appearance. The presence of these basic patches has doubtless aided in the production of the distinct banding of the granitic gneiss during the process of dynamic metamorphism. In this connection the writer has read the recent paper! by Professor Adams which deals with the origin of the amphibolites in the Glamorgan gran- ite of Ontario, Canada’ og: les - : ; s ea po ties hh * ‘ : ; . t ® ‘4 - ? sa «. 1 = : 2 ‘ E She ; 2 S 2 E A , ¥ > fs e ; \ * oy } S i) ; , } F ' 5 ) 1 ‘ } es & =n 784: GEOLOGY OF THE PORT LEYDEN QUADRANGLE 19 are quartzose and garnetiferous may be accounted for by some such process. ) Three syenite-Grenville areas are shown on the map. The largest of these extends from Denley station to north of Greig, a distance of nearly 12 miles, while the width averages some- thing like 3 miles. In the southern portion of this area the Grenville is present in greater force than the syenitic or granitic rocks, while in the northern the reverse is true except possibly in the vicinity of Greig. Within this area there seems to be good evidence for the former existence of very ancient Grenville rock belts or structure lines which extended in a northeast-southwest direction. Thus pyroxene gneisses are found in the area east of Fowlersville; in small outcrops 1% miles east of Port Ley- den; and 14%4 miles north of Denley, and these are all arranged along a northeast-southwest line. A belt of feldspar-garnet gneisses shows a similar strike and extends from Lyonsdale to Port Leyden. Quartz-sillimanite rocks much like those at Kos- terville have been noted in small exposures from % to 3% of a mile north of Port Leyden and this suggests another northeast- southwest belt.. A less well defined belt is garnetiferous and passes through Lyons Falls. Still another belt, in which garnet- sillimanite gneisses are commonly found, passes northeast and southwest through Greig. It seems pretty certain that before the intrusion of the syenite, these Grenville belts were continu- ous and well defined and that as a result of the intrusion they were all cut up leaving only here and there masses of the pure Grenville. Of the two smaller syenite-Grenville areas, one lies about 2 miles north of Fowlersville and the other around East Martins- burg. These rocks are quartzose syenites often containing gar- nets and more or less intermingled with Grenville. The great variety of rock types making up this complex and their gradations from one type to another make it difficult to give a proper idea of them by description. Microscopic study of numerous thin sections shows the presence of all the minerals of both the Grenville and the syenite and in addition to them microcline which often occurs as a prominent feldspar. The fol- iowing brief descriptions include most of the leading types: I Syenitic facies. These are often practically indistinguish- able from the normal syenite. They are usually, however, pretty fine grained and under the microscope nearly always show a highly cataclastic structure. They frequently contain microcline 20 NEW YORK STATE MUSEUM feldspar and a large proportion of quartz and the dark colored minerals. Thus a specimen from along the railroad 2% miles north of Lyons Falls contains 75% of microperthite; 20% of quartz; 5% of magnetite, biotite and hornblende, together with a little zircon. Another from % of a mile southwest of Goulds Mill contains 65%, in about equal amounts, of microcline, micro- perthite and plagioclase (oligoclase to labradorite); 25% of quartz; and 10% of biotite and magnetite. North of Lyons Falls, along the railroad, similar rocks often carry 30 to 40% of quartz with sometimes a little anorthoclase and they greatly resemble the granitic syenite. 2 Grenville facies. Small exposures often show very pure Grenville as for example at the river dam 1% mile north of Port Leyden. A thin section from here shows 80% quartz; 109% silli- manite; 8% magnetite and 2¢ biotite, together with a little zircon. Again, a typical pyroxene, quartz gneiss is associated with syen- itic rocks 14% miles above the mouth of Miller brook. A Grenville facies carrying garnets occurs in the vicinity of the paper mill at Lyons Falls. 3 Garnetiferous gneisses with a general igneous appearance are very common. Such a rock 2 miles east of Port Leyden shows 65% of microcline and microperthite; 20% of quartz; 5% of hornblende and biotite and 10% of augite, magnetite, garnet and zircon. A similar type much richer in garnet and almost free from dark minerals occurs in the river bed at Port Leyden. Anotherige from 2% miles east-southeast of Greig shows 65% of plagioclase (oligoclase to labradorite) ; 30% of quartz and 5% of biotite, gar- net, magnetite and zircon. The origin of these gneisses is doubt- ful but they may have been formed by a thorough mixing of Grenville masses with the molten syenite. The garnets in these rocks are frequently an inch or more across. 4 A very gneissoid, rather dark rock, which is fairly common, is rich in plagioclase, quartz and biotite. An example from % mile south of Lyons Falls contains 45% of plagioclase (oligoclase to andesin) ; 40% of quartz; 10% of biotite; 2% of hornblende and 3% of magnetite, zircon and pyrite. 5 A very gneissoid, dark rock from 144 miles east of Port Leyden contains 50% of microcline and plagioclase (oligoclase to labradorite) ; 20% of quartz and 10% each of green augite, biotite, magnetite and a very little garnet. 6 A type of dark, quartzless, gabbroic rock such as that at Lyons Falls dam contains 55% of plagioclase (oligoclase to labrador- . ‘SOSSIOUS POXIUW I[[TAUSID) “o}USAS 94} YIM poddeim wseq sey YSIYM sseUl IOIqqes “YIep & St o194 YOO1 OY], ‘s[[ey SUOATT 3e JOATI Youyg fo sypey v 93e1q “if eae ray. GEOLOGY OF THE PORT LEYDEN QUADRANGLE 21 ite) ; 40% of green hornblende and green augite and 5% of hyper- sthene, magnetite, biotite, zircon and apatite. This type is in contact with another gabbroic rock which has a considerable percentage of quartz and hypersthene and some microperthite. 7 Very dark, long, narrow patches which are probably inclu- sions are common. They usually consist mostly of decomposed hornblende and basic plagioclase together with some quartz, magnetite and biotite. Undetermined Precambric areas Unfortunately several large Precambric areas are so deeply buried under Pleistocene deposits that the character of the un- derlying rocks is entirely unknown. These areas have been so indicated upon the geologic map. EO ZOl ROCKS The Paleozoic rocks occupy a little over one half the area of the quadrangle on the west side. Except at the extreme south they always lie to the west of Black river. The maximum thick- ness of the Paleozoic formations is approximately 1500 feet. Potsdam sandstone The Potsdam sandstone is of upper Cambric age and is the most ancient sedimentary formation bordering the Adirondacks. It is not present in outcrop in the Port Leyden quadrangle nor in fact along the whole southwestern border of the Adirondacks, although it is most likely present beneath the later formations. South of Port Leyden the deep wells at Utica and at Rome show a basal sandstone which is more than likely the Potsdam. West Sie ore Leyden the Potsdam, according to Orton,! is most cer- tainly present in the deep wells of Oswego county at Central meeare atisn, Pulaski and Stillwater. The nearest outcrops of the sandstone are something like 20 miles north-northwest of the Port Leyden quadrangle and from there northward to the St Lawrence it is a common surface rock. Pamelia limestone The Pamelia limestone was named by Professor Cushing from a town in Jefferson county where he recently recognized it as a. distinct formation.2, Between the Potsdam and the Pamelia, * Petroleum and Natural Gas in New York. N. Y. State Mus. Bul. 30. 1899. | Geol, Soc. Am. Bul. 1908 19:155-76. 22 NEW YORK STATE MUSEUM in the St Lawrence and Champlain valleys, other formations come in whose exact relationships have not yet been made out. According to Ulrich the Pamelia is to be correlated with a part of the Chazy of the Champlain valley. For a long time the Pamelia had been described and mapped as Beekmantown lime- stone, but it now seems to be pretty well established that the true Beekmantown is not present along the northwestern Ad- irondacks. The Pamelia formation (Lower Siluric) is the oldest sedi- mentary mass exposed within the limits of the quadrangle. Its outcropping edge, which extends from north to south across the district, everywhere rests directly upon the Precambrie rocks. Since it outcrops at the base of the steep slope facing Black river its surface exposure is small. The actual contact with the Precambric may be seen in at least three places as follows: Where the railroad crosses Roaring brook near Martinsburg station; along the creek 114 miles northwest-north of Lyons Falls; and along the railroad 34 of a mile north of Port Leyden. At a number of other places the contact is almost visible. The bed in actual contact with the Precambric is always a sandy conglomerate above which occur several feet of calcareous sand- stones, then a few feet of bluish black, fossiliferous limestone, and finally thin to thick bedded, whitish gray to bluish gray, rather impure limestones which latter make up more than half the section. Many of the upper, gray beds are really magnesian limestones which may be burned for waterlime as has been done at Lowville. The conglomerate and sandstone at the base of the Pamelia represent the materials derived from the Precam- bric land surface as the sea encroached upon it. According to the observations of Professor Cushing on the Theresa quadrangle (northward), which are corroborated by the writer on the Port Leyden quadrangle, the basal conglomerate and sandstone rep- resents a shifting upward horizon, due to overlap, as the sea encroached upon the land from west to east. These basal beds are more than likely to be correlated with the Rideau sandstone as described by Ami in Ontario, Canada. Following is a detailed section: made by Professor Cushing along Roaring brook (near Martinsburg station) and kindly fur- nished to the writer: 4 inches of blue gray calcareous shale above and 9 inches of eet Inches same beneath with a 4-inch layer of mottled blue limestone like that Dberieath cis 2o'0c)s sjelciereusl ace retetetetnterenciet terete soielal=a0a pela tate I 5 ih W. J. Miller, photo View along Black river, 1% miles above the mouth of Sugar river, taken to show the sharp contact between the Trenton and the Black River limestones. During high water the thin bedded Trenton lime- stones have been worn back to leave exposed a distinct platform of the underlying massive Black River limestone. | 1p tes i 7 ‘ =I Pa 4 ? ) 1 y \ tS { y - . Plate 6 oo a: W. die Muller, . photo A group of “potholes” in the bed of Sugar river % mile below the railroad crossing. The rock is Black River limestone. i; iat wee) > es GEOLOGY OF THE PORT LEYDEN QUADRANGLE A massive bed of blue granular limestone, mottled and lam- inated and with pebbles of blue dove limestone............ Hard, gray white limestone with spots of crystallized calcite.. Bluish gray, thin bedded limestone, with ripple marks and Es cle eG ck cc csi ce os cuecsvevcieees Shaly, dirty white mud limestone beds, mud cracked........ Pemcmeswbetaniar, thin bedded limestone........:.......... Blue dove, hard, mottled limestone, shaly below, traces of ee I Sire ct te cage tg we bb het Se do eo ew see Hard, gray granular limestone, pinkish tinge, much calcite.. Thin, ripple marked, dirty white, mud limestone beds........ Hard, blue gray subgranular limestone, sand grains and ostra- IR IS Se ei ig Sieg, Gielnis 4 os Gos nm ince eves Hard, gray white limestone, less earthy than usual; calcite a Eric Ais Pola Kia) se /ccl/s/o/c/a) soe es ae se vies ss eye cle a's wiv Subgranular, blue, laminated limestone; welded contact with oS oie ss cle cco ee.d cowie ee Vee ieaeevuceens Very massive, gray white, earthy limestone, irregular splitting. Massive blue dove limestone in two layers; laminated; sty- MMT EIIBEAIGCES OL TOSSIUS .. . csc cca ce cs cee eee caeedesas Thin and thick bedded, blue subgranular limestone; massive Peemewer jamimated: mich mud cracked................ Earthy, impure, gray white beds; massive and irregular split- ting; lower 12-18 inches hard, gray white, calcite spotted, ERT ene. caso ay sa Psion a wineis's Se bipe'b eve ee Graeme, impure, earthy, blocky beds..............5.0.00% Impure, gray white, reddish tinged, earthy limestone, with purer layer of reddish limestone at base; quite massive; NE EM a aces oc ise) ade daw epee ete we be viet s Bluish black, fine, hard limestone, like 2d beneath but unfossil. Gray to blue gray, magnesian looking limestone in 3-6-inch ee ee te cee eelna nese eee es 3 heavy layers of hard, bluish black limestone; ringing; multi- tude of small fossils, lamellibranchs, cephalopods, one- SU SeeeeMNIELTRCTG Ms ks cn cn be cle eee ee ee ence Red and green, impure, calcareous, sandy mudstone, large sand grains; upper 6 inches thin bedded, rest massive.......... Very sandy firm green limestone, full of quartz grains...... Hard, gray white, somewhat sandy limestone or dolomite; Re wc bce c dase a vepeeeees Peemetineiie oteen, calcareous sandstone............+.s2..: Mme er Ofetl (Shale... 4. bck ce cee ee ewe ecw aeeus More solid, red and green calcareous sandstone; rots easily.. Red and green, rotten, calcareous. sandstone................. Feet Seeeteana ted atkose; perhaps calcareous.................-. Beenemterate testing on Precambric............0.cuscassece Total See FT see ee et sete secscoeovestoanueecet sevens eneteovoseseveeeceeneevee 23 Inches eeeseece 24 NEW YORK STATE MUSEUM Eight miles south of the above section and 1% miles north- west-north of Lyons Falls station another excellent section is shown along Mill creek where all the beds from the Precambric to the Trenton are exposed. Mill creek is not propery, placed on the map here. Its true course is close to the town line be- tween Turin and West Turin. By means of the hand level the writer has determined the thickness of the Pamelia here to be about 56 feet. The basal conglomerate, 1 foot thick, 1s followed by 10 feet of gray, calcareous sandstones and very sandy lime- stones with some sandy shale partings. Next come 4% feet of bluish black limestones. Above this the beds are much like those along Roaring brook and their summit is here also capped by a limestone conglomerate. 7 Some 7 miles south of the Mill creek section and in the vicin- ity of Denley there are good exposures of the Pamelia. No complete section is visible but a study of all the outcrops makes it certain that the formation is here not over 20 feet thick: | Tite basal conglomerate and sandstone underlies grayish, sandy, thick bedded limestones, while the whole is capped by the usual lime- stone conglomerate. The most southerly outcrops of Pamelia occur along Mile creek from ¥%4 to 1 mile above its mouth, where the formation is apparently not over 10 or 12 feet thick. It dis- appears before the Remsen quadrangle is reached. The thinning out to disappearance of the Pamelia in passing southeasterly may be entirely explained as due to overlap, since the formation came in from the west, as above shown, and rap- idly thins out eastward. Its place of disappearance, most likely in the northeastern corner of the Boonville quadrangle, is some 9 or 10 miles east of a north-south line passing through the Roaring brook section where the Pamelia is over 71 feet thick. This represents an eastward thinning of 7 or 8 feet per mile which compares favorably with the rate of thinning noted by Cushing over the Theresa quadrangle. Of course, some of the thinning may quite possibly be due to a lack of deposition_of so much material in. the southern portion of the basi) Iijseemme certain that the Pamelia is present in considerable force, under cover ‘of later rocks, in the western’ part of the Por) Weyaen quadrangle and to some extent, at least, in the northern part of the Boonville quadrangle. In a letter Cushing says that what has heretofore been referred to as Beekmantown-Lowville passage beds in the region around Little Falls may in reality be a touch of the Pamelia there. ‘QUOJSOUM] WOJUIIT IUL[e}sh19 pappoq AAvoy JoyJeI SI YOO YT, ‘aspriq peospresr oy} 2Aoqe ysnf JoATI IeSNS jo syey ‘ -t GEOLOGY OF THE PORT LEYDEN QUADRANGLE 25 Lowville limestone The Lowville limestone formation takes its name from the type locality at Lowville a few miles beyond the map limits to the northward. It was formerly called the Birdseye limestone because of the spotted character of the surfaces due to the emer- gence of the calcite-filled tubes so characteristic of the formation. These calcite-filled tubes stand perpendicular to the stratifica- tion planes and were first thought to have been caused by a seaweed of the Fucoid type, but they are now referred to the genus Tetradium of the branching corals. Not all of the Low- ville beds contain the Tetradium. In the old State report by Vanuxem everything below the Trenton, in this region, was described under the heading “ Black River limestone,” but the following quotation shows that, on lithologic grounds, he recognized three divisions of the forma- tion: “ The cliff shows several distinct kinds of limestone, not being a homogeneous mass. The upper part is mixed irregularly ae black shale. ... The second division is of a lighter color, with less shale or impurities, more brittle, and contains Sememcoetdes demissus (Tetradium), etc. . . The third division, and which therefore forms the base of the cliff is light colored, and the surface of some of the layers present mud cracks, showing the presence of shale. It is in these layers that the stone exists which is burnt for waterlime at Lowville.”1 His upper division corresponds to our Black River limestone, the middle one nearly to our Lowville, and the lower one nearly to our Pamelia. Within the map limits the Lowville, together with the Pam- elia, is Present, except at the extreme south, as an almost con- tinuous surface exposure or ledge facing the railroad. In spite oi its considerable thickness its areal extent is small because of its outcrop along this steep slope. The Lowville beds are mostly bluish dove-colored, pure limestones in beds varying from a few inches to 2 feet thick. Some of the beds are mud cracked, others are shaly, while still others are fossiliferous commonly with the Tetradium. A notable feature is the pres- ence of limestone conglomerate at several horizons. In passing downward this conglomerate is prominent where the pure dove limestones give way to the more impure bluish gray to whitish gray limestones and it is here where the line between the Low- ville and Pamelia has been drawn. Within the quadrangle this line is a difficult one to draw with any great degree of accuracy. sarcol. N. Ys 3d Dist. 1842. p. 42. 26 NEW YORK STATE MUSEUM According to the work of Cushing and Ulrich farther northward, there is an unconformity separating the two formations, the time gap being represented by the upper portion of the Chazy of the Champlain valley. In the Port Leyden district, the change from the conglomeratic bluish dove limestones to the more im- pure whitish, sandy beds seems significant and may be due to an unconformity at this horizon. Certainly, however, the writer has found no evidence of any well defined or large unconformity between the Lowville and Pamelia. In the Roaring brook section as measured by Cushing the Lowville is made up as follows: Feet Inches 6-foot layer of Black River limestone; upper 3 feet full of ‘ CHET oc eia ai earthetees ilk Sle Gn eee een Re ct ae Pe aaa es os Mostly thin bedded blue dove limestone in 6-inch to I-foot layers, full of Tetradium and other fossils, to base of Black Massive beds of blue dove limestone in 18-inch to 2-foot layers; only sparingly fossiliferous, but more or less Tetra- dium’ everywhere) «2 eee ete ies roe sialon e oe in 4 Shaly, ‘blue dovetlanestonme: syseeerer rin Coes oe eer cee I 8 Blue, granular limestone full of fossils and much crystallized Caleite Yaccesea SoG tiek Se Be eee ee tacos ett I 2 Ordinary blue dove limestone; lower portion full of gastro- pods; upper portion a limestone conglomerate with bunchy surface and Stromatocerium look; filling in above are 2~-I0 inches: of vshaly dimestome,ts.ceie cite eee eee oe wc ee 2 10 Thin bedded blue dove) limestones. meee eres: ond oss ieee I I Massive blue dove limestone; few fossils and little calcite.... 2 ah Blue black dove limestone; full of fossils and crystallized cal- Cite stim peddedis Shaly " pee ' Whitaker falls on Roaring brook 1 mile southwest of East Martinsburg station. The rock is Trenton limestone. f ¢ . e } \ es — 2 ‘Re ‘fake ‘ F - Soe Lea tia + Tx i ; . ie CRAG : oie F : ¥ 7 a ft ¢ fe vy ; aie - v 4 a . S A i 1 f 4 f ‘ \ by: e : : a ft i ‘ ; } GEOLOGY OF THE PORT LEYDEN QUADRANGLE 31 The thickness of the Trenton has been paar) determined in a number of places as follows: Feet peemeeiecse creek and Sugar river.......3..... ese eee 350 Between Port Leyden and Locust Coa Seer eer: ZO Rt ELCCK 6. ke ee ee (ohare ach Caeser 400 y Soee RSS ae SE 2s 450 Along Roaring brook and Atwater eee BNR OR Potties AE 475 Thus, in a distance of 20 miles across the map, from south to north, the Trenton shows an increase in thickness of something like 125 feet or at the rate of about 6 feet per mile. Passing south- eastwardly along the line of outcrop, the Trenton shows a progress- ive thinning. Thus at Remsen it is about 300 feet; near Middleville 200 feet; at Ingham Mills 100 feet; and at Canajoharie only 17 feet. Westward in Oswego county deep wells at Stillwater and Central Square show respective thicknesses of 670 and 747 feet. Utica shale The Utica shale formation shows practically the same character- istic features here as it does at its type locality at Utica. It is a very fine grained, dark gray to black, thin bedded shale. The black color is due to the presence of carbonaceous matter which may be readily burnt out, although, contrary to a current popular idea, nothing like a workable coal seam occurs within the formation Occasionally some of the layers are rather sandy especially toward the top. Toward the base of the formation some of the layers are several inches thick and are frequently calcareous and except for this the contact between the Utica and the Trenton is a sharp one. Because of the softness of the rock and the character of the out- crop, favorable to the development of talus slopes, the actual con- tact between the shale and limestone was nowhere observed. Manv times, however, Trenton beds have been noted in such close prox- imity to the shale that the boundary line can be pretty accurately drawn. Such observations may be made along Atwater creek or Moose creek. In spite of a considerable thickness its areal extent is rather small because it outcrops along the base of the steep slope forming the eastern fronts of Tug and Mohawk hills. Excellent sections are to be found along all of the larger streams which cut across this steep slope. Its broadest surface exposure is from Constable- 32 NEW YORK STATE MUSEUM ville southward where the shale is thickest and the slope is not so great. An interesting erosion remnant, or outlier, separated from the main mass covers several square miles in the vicinity of Locust Grove. | The Utica shale is here not highly fossiliferous although certain fossils so common to the formation may be found in nearly every exposure. Among these are the Endoceras proteiforme of the. chambered cephalopods, Driarthrus bee aromerne trilobites, and some graptolites. Animal life in the Trenton ocean was very prolific, but with the advent of the muddy Utica sea there was a great diminution in both the number of species and individuals. | Along the line of outcrop the shale shows a notable and steady decrease in thickness toward the north. Following are approxi- mate determinations of the thickness within the quadrangle from south to north. Feet Along’ Moose:creck 7a. oa nee ee 300 At Constablevalle: tof yee eee eit aie aes a ae 260 Aut arin ate pe ate, eee ee a ley Pee oenme meriesrs 230 At Houseville 205.00 oa eee en eee 200 Along Atwater -creelig) 7 ee ee ee ee 180 Southeasterly along the line of outcrop the Utica increases in thickness. Near Remsen it isvover 30 feet and near [eile sams about 600 feet. Westward in Oswego county it shows a thickness of 180 feet at Central Square; 120 feet at Fulton and auaprceemet Stillwater in the deep wells. Thus it is evident, in a general way along the southwestern Adirondacks, that the Utica is thinnest where the Trenton is thickest and vice versa, the two formations having nearly the same thickness on the Remsen quadrangle. Lorraine shales and sandstones The Lorraine formation received its name from the town of Lor- raine in Jefferson county, some 30 miles northwest of Port Leyden. The rocks included under this heading are the same as those of the old “ Hudson River group” of Vanuxem’s report.1 In the future the Lorraine beds will doubtless be subdivided, but more detailed work over a wider territory must be done before such subdivision is attempted. In the meantime, all the strata lying between the 1Geol. N. Y. 3d Dist. 1842. p. 60. ‘QUIVIIOT 9s} JO SouO|spuesS PUR so[eYs SuT}eUIDz[e 943 IIR Sy901 Pesodxa pue jyoofy Oo€ Ajieou St YWdep OY] “JOMOIIEU YONUI ST FINS oy} sly} osAoqe souRIsIp JOYS WY “f[NSs GuUO}S}OY AA UI MoIA VY GEOLOGY OF THE PORT LEYDEN QUADRANGLE 33 Utica shale and the Oswego sandstone, two well marked horizons, are described and mapped in this report as Lorraine. The formation consists chiefly of alternating thin bedded shales and sandstones together with some thin layers of limestone. There is no sharp line of separation between the Utica and the Lorraine, the lowermost shale beds of the Lorraine being in every way like those of the Utica. The lower Lorraine, comprising a thickness of approximately 200 feet of shales, is not very fossiliferous and contains occasional thin beds of fine grained sandstone. Among the ioiwine Bmdoceras proteiforme and Triarthrus becki, so common in the Utica shale, are also found here. The lower Lorraine as thus described corresponds in a general way at least to Vanuxem’s Frankfort slate and sandstone.! The upper Lorraine, showing a thickness of something over 400 feet, is made up of gray, fine grained sandstone beds alternating with black to dark gray shales and occasional thin beds of impure limestone. Passing upward the sandstone content increases greatly and the thin partings of shale become rather sandy and light colored. The upper Lorraine sandstones and limestones are highly fossiliferous and fragments of sandstone full of fossils are strewn over the Tug hill region in great quantities. Among the many mses some of the more noteworthy forms are: Penta- emadtes hamptonii of the echinoderms, Leptaena memteed atid Orthis testudinaria of the brachiopods, Ambonchyia radiata and Modiolopsis modiolaris @eetie lamellibranchs and Cyrtolites ornatus of the gastropods. A more complete list of fossils for this general region may be found in a paper by Walcott.2, The upper Lorraine as here described corresponds roughly to the sandstone shale of Pulaski as used in Vanuxem’s report. From the standpoint of both areal extent and thickness the Lor- raine is the principal Paleozoic formation of the quadrangle. Ex- cept for the small Oswego sandstone area, the Lorraine occupies all of Tug and Mohawk hills. Fine sections are exposed along the larger streams which cut across the eastern front of Tug hill, the best one probably being in Whetstone gulf [see pl. 9]. The whole thickness of the formation is shown in the township of Turin where it is estimated at 630 feet. About 600 feet are shown in Mohawk hill with the top not present. Well records to the west and south pac, cu. Dp. 6r. *Geol. Soc. Am. Bul. 1890. 1:348-49, | ree een 34 NEW YORK STATE MUSEUM ‘show the Lorraine to be 600 feet thick at Lorraine (Jefferson co.) ; 530 feet at Stillwater (Oswego co.); 549 feet at Central Square (Oswego co.); 640 feet at Chittenango (Madison co.) and 720 feet at Vernon (Oneida co.). According to these figures there is somewhat of variation in thickness but not in any particular direction. Oswego sandstone This formation is so named because of its prominence in Oswego county. It is the only representative of the Upper Siluric within: the quadrangle, and corresponds to the gray sandstone of Oswego as used in Vanuxem’s report. But one small area occurs within the map limits and this forms the capping of the highest part of Tug hill. This area represents the easternmost extension of the formation which occupies many square miles in the southern part of Lewis county. The Highmarket quadrangle, immediately to the west, is literally strewn with slabs of this sandstone and the region is characterized by numerous swamps and a sluggish drainage. Within the map limits the Oswego sandstone is a gray, fine grained, thin bedded rock. The stratification is not very regular and practically no shale is present. Fine examples of cross-bedding on a small scale are common. A characteristic feature is the presence of occasional yellowish spots of limonite, which are no doubt due to the alteration of original iron pyrite. In marked contrast to the underlying formation, the rock examined appeared to be barren of fossils. The sandstone lies between the 2000 and 2100 foot con- tours, thus showing a thickness of about 100 feet but with the top not reached. STRUCTURAL GEOLOGY, Dip of the Paleozoic formations Movements since the deposition of the Paleozoic strata have given them a very perceptible dip toward the southwest. This dip may be determined, in a general way at least, by comparing the alti- tudes of given horizons within the Port Leyden quadrangle and south and west. For this purpose the top of the Trenton is chosen because it is so clearly recognized in well sections. : The top of the Trenton in the Rome well, as reported by Prosser," is 205 feet below sea level, while 2 miles west of Port Leyden it is *Am. Geol. 1900. 25:137. GEOLOGY OF THE PORT LEYDEN QUADRANGLE 35 1280 feet above sea level. Thus in a distance of 25 miles the top of the Trenton drops 1485 feet or shows a southerly dip of nearly 60 feet per mile. Pecerdiae to Orton, the top of. the Trenton in the Central Square (Oswego co.) well was struck at 1209 feet below sea level. The same horizon 2 miles west of Port Leyden is at an altitude of 1280 feet above the sea which thus shows an increased elevation of 2489 feet within 44 miles or a southwesterly dip of over 86 feet per mile. : In the Stillwater (Oswego co.) well Orton? reports the surface of the Trenton at 25 feet below sea level and this is 1305 feet below the same horizon 2 miles west of Port Leyden. The distance is 30 miles and the westward dip is over 43 feet per mile. Within the map limits, near Locust Grove, the Trenton-Utica con- itera atan cleyation of nearly 1300 feet, while 2 miles to the southwest it is a little over 1100 feet, thus indicating a sotithwest- ward dip here of about 50 feet per mile. An exceptional dip of 3 or 4 degrees toward the southwest nay be seen in the Trenton limestone in the vicinity of Martinsburg. This is probably due to the updrag effect of the fault below described. Faults and folds No fault of sufficient extent to be mapped has been found within the limits of the quadrangle. A few places have been noted where there have been slight movements of I or 2 feet as for example in the Trenton of the Black river gorge 2%4 miles northeast of Boonville. : Just beyond the edge of the map and in a ravine 3% of a mule northwest of East Martinsburg station a fault with considerable displacement is well shown. No detailed study of this fault has been made, but it is of the normal type and strikes approximately northwest-southeast. Its length was not determined. The fault plane stands nearly vertical and the limestone beds are highly in- clined on the south side as a result of the updrag during the process of faulting. On the north side of the ravine the Precambric lies fully 40 cr 50 feet higher than on the south side and this represents the amount of the throw. The Pamelia beds have been faulted against the Precambric. The unusually rapid downward slope of IN. Y. State Mus. Bul. 30. 18009. p. 455. 2loc. cit. p. 448. 36 NEW YORK STATE MUSEUM the Precambric surface between Glenfield and East Martinsburg is due to the settling of the mass on the south side of the fault. Extensive folding of the Paleozoic rocks nowhere occurs. Local iolds are sometimes developed but even these are rare. Such smal! folds are best seen % mile above the mouth of Mill creek (north of Boonville) ; near Denley; and where the railroad crosses Sugar river. At the latter place a syncline in the Trenton is perhaps the best example of folding in the district. The folded structure of the Precambric rocks will be dealt with under the heading “ Gneissic structure.” Ripple marks Small ripple marks are frequently present in the Paleozoic forma- tions. Thus at several horizons within the Pamelia, Lowville and Trenton limestones there are ripple marks which measure I or 2 inches from crest to crest and about % inch from trough to crest. Special attention, however, is called to certain ripple marks of un- usual interest 11 the Trenton:: They are of unusual imterest bork because of their large size and their occurrence im > Mmwesteme: These marks occur about 25. or 30 feet above the base @raeie Trenton and are finely shown in the south bank of Sugar river a short distance above the railroad bridge. The ripples measure from 24 to 56 inches from crest to crest, and 4 to 7 inches maou trough to crest. hey strike about n. 30° €. The ripple masked layer varies in thickness from 2 to 9 inches and is a crystalline and very fossiliferous limestone. Shale occurs immediately above and below the marked stratum and the shale above- thickens or thins according to whether it rests wpon the troughs or crests of the ripples. The limestone layers both above and below rapidly thicken and thin and are certainly of shallow water origin. Gneissic structure The precambric rocks, which are metamorphosed, igneous and sedimentary masses, all exhibit the gneissic structure. This struc- ture is best developed in the old Grenville sediments and least in ~ the syenite. In the areas of mixed gneisses it is also clearly shown. The strike of the gneissic bands varies from north-south to almost east-west, but the most common range is from n. 40° to 70° e. The direction of dip of the foliation planes is either northward or southward but prevailingly northward. The angle of dip is usually high, varying from 50 to 80 degrees although just north of Lyons : : GEOLOGY OF THE PORT LEYDEN QUADRANGLE 37 Falls it is as low as 20 or 25 degrees. From south of Denley to 3 miles north of Lyons Falls the dip is northward; thence north- ward to just south of Glenfield it is southward; thence northward to the map limit it is northward. Thus we have good evidence of distinct folding of the Precambric rocks on a large scale. Certain other Precambric rock structures will be discussed later. Structure sections The structure sections shown in figures 2-4, page 38, have been carefully chosen with the idea of giving the best general notion of the various rock formations and their relationships to each other. PALEOZOIC OVERLAP It is well known that during the general subsidence (barring cer- tain minor oscillations of level) of the Adirondack region in early Paleozoic times, sediments were being deposited on the Precambric surface and that these sediments gradually encroached upon the sinking land mass until nearly all, if not all, of the Adirondack region was covered by them. The younger formations extended farther in than the older ones upon the sinking surface, thus con- stituting an overlap of the Paleozoic sediments upon the Precambric crystallines. The stripping off of this Paleozoic cover has been going on since the close of the Paleozoic era, at least, and the exposed surface of the Precambric rocks is still being enlarged by this same process. A glance at the structure sections [fig. 2-4] will show the eroded edges of about 1500 feet of sediments which formerly must have extended farther eastward upon the Pre- cambric stirface.. In the Port Leyden district we have positive evi- dence to prove the Paleozoic overlap. On the western side of the Adirondacks the oldest overlapping formation is the Potsdam sandstone. It is not present in outcrop within the Port Leyden quadrangle, the nearest exposures being about 20 miles northward in the vicinity of Carthage. Accord- ing to Orton! the Potsdam, resting upon the Precambrics, occurs | in Oswego county to the west and southwest of Port Leyden as shown in deep well sections. Thus the deep well at Central Square Shows 156 feet of sandstone; the well at Parish 50 feet of sand- stone and the well at Stillwater (southeast of Orwell) at least 49 *N. Y. State Mus. Bul. 30. NEW YORK STATE MUSEUM 38 SB sles 94} ole SjoqwAS sy J ‘TeJUOZIIOY 9y4 ‘dew o1so0joes 94} uo pozvol SOIMY SI B[BOS [BOI}IeA ‘dew o1s0[0e3 943 uO 9soyy put ere soul] UOTJOeS oY, + “e[suvIpenb usepso7T Od 94} SsOlov suoltjoes ainjoni4¢ 22h) ONES) eS Gr hel 48UV7 INE) Tb Que Reed a) apa v—z GEOLOGY OF THE PORT LEYDEN QUADRANGLE 39 feet of mostly sandstone. Orton refers all of these sandstones to the Potsdam. The bottom of the section at Stillwater is: Feet Ere offen ee oe eee ee ee natee 370 WMT oe i ec ee ee eee nee eus 4O CWE ee ce ee eee 25 PC MINMESEONG. 2... oc eke ee hehehe, Send et Beg 5 Meeeiaenmiitke Satiastone, calcareous. ..........2..00e00ee 18 REM MSEC AL ee ee es oe ce ede 1697 Fossils in the black limestone layer prove the Upper Cambric (Potsdam) age of the deposit. The presence of this Potsdam in Oswego county and its absence along the Paleozoic-Precambric boundary to the eastward on the Port Leyden sheet, SIEOEE con- clusive evidence of overlap. Again, we have a strong argument in favor of overlap if we con- sider the whole thickness of sediments between the top of the Tren- ton and the Precambric. Details will be presented later, but suffice it to say now that a comparison of the thickness of these sediments in Oswego county with those near Port Leyden shows a thinning of several hundred feet in passing toward the latter place. Such a marked diminution in thickness toward the northeast and east is just what would be expected in the case of overlap. SUR PACH OF THE PRECAMBRIC ROCKS Smoothness of the surface which received Paleozoic deposition A study of the Paleozoic-Precambric line of contact gives strong evidence in favor of the statement that the sinking surface which received Paleozoic sedimentation must have been worn down to a remarkably smooth condition (peneplain). Except for a few miles near the southern edge of the map, the Paleozoic-Precambric boundary line can be drawn with a considerable degree of accuracy. A glance at the geologic map will show that this boundary line is a very regular one which at no point shows any rapid elevation or depression. Such a regular line of contact is precisely what one would expect where sediments have been laid down upon a smooth floor and then, after elevation, have been stripped off rather regu- larly by erosion. Even a comparatively small elevation or depres- sion along the contact line could be recognized. At several points where the actual contact is exposed, the Precambric floor appears to be smooth. 40 NEW YORK STATE MUSEUM Because of the deep mantle of sand and gravel which now covers the Precambric surface east of Black river, the configuration of that surface can not be studied to the best advantage. But so far as can be judged, if the stream channels in the Precambric surface were filled up the resulting surface would be comparatively smooth and even which strongly argues for that sort of a surface before the stripping off of the sediments and later erosion. Any prominent elevations on the old floor ought now to be recognizable, especially in the valley bottom and near the Paleozoic boundary, but none occur there. The distinct rock ridge southeast of Fowlersville seems to be the only example of such an elevation. This ridge rises abont | 80 feet above the general level but its hight is thought to have been somewhat accentuated by tce action. Again, if there had been any marked depressions in the old floor they would have been fille up with Paleozoic sediments and we might well expect to find such protected sediments as isolated patches or outliers within the gen- eral Precambric area as, indeed, the Potsdam sandstone does occur - some 30 or 40 miles farther northward. The available evidence, however, points to a complete removal of the sediments. The conclusion for the Port Leyden quadrangle is that the Pre- cambric floor upon which the sediments were laid down was com- paratively smooth and even, with only one known elevation rising above the general level. This is substantially the conclusion reached by Professor Cushing and the writer for the Little Falls and Rem- sen quadrangles respectively and it is true of the southern and south- western border of the Adirondacks. This result as Cushing says “seems specially important in view of the fact that Professors Kemp and Smyth, and the writer (Cushing) also, have found evi- dence to show that, in the St Lawrence and Champlain valleys and vicinity, the surface on which the Potsdam was deposited was con- siderably more uneven than this. In other words, the surface to the south was worn down to a nearer approach to base level than was the case farther north.” Slope of the Precambric surface where now exposed We have just shown that the Paleozoic sediments were deposited upon a very smooth Precambric surface. The uneven and dissected character of that surface where now exposed is due almost entirely to erosion since the stripping away of the sediments. Since the above was. written Prof. H. L. Fairchild has presented several papers, bearing on the glacial history of northern and central New York, before the 1908 meeting of the Geological Society of America. ‘These papers will be published in the bulletin of the society GEOLOGY OF THE PORT LEYDEN QUADRANGLE A5 even the hardest rocks, exposed during all of postglacial. time, have been weathered enough to cause an obliteration of the glacial marks. | Striae pointing from s. 25° to 40° e. have been located as follows: On Trenton limestone 1 mile south of Martinsburg and also % mile to the east of that v‘llage (s. 25° e.); on Black River lime- meeeise west of Lyons Falls; on Precambric near the mouth of Roaring brook, 1% miles northeast-north of Glenfield and also % mile southwest and 34 mile southeast-south of the same vil- lage; on Precambric 1 mile northeast of Denley and % mile north- east of Hawkinsville. Striae bearing nearly south occur on the Pre- cambric 1 mile east of Port Leyden. The southeasterly movement, shown by these marks, changed to a more nearly easterly move- ment in the Mohawk valley region, and this is just what would be expected according to the statement of Chamberlin. It should be noted that the Black river valley, which is the chief topographic feature on the western side of the Adirondacks, had much to do with determining the direction of flow of the ice. This valley existed in preglacial time and the close parallelism between the directions of the striae and the direction of the valley shows the influence of the latter in determining.the ice movement. Along the northwestern border of the Adirondacks the ice undoubtedly moved southwestwardly. Along the eastern border of the Adirondacks the general southerly movement of the ice has been well established, as has also the westerly movement up the Mohawk valley toward Little Falls. Thus the statement of Chamberlin, regarding ice flow around the Adirondacks, harmonizes almost perfectly with the observed striae. | But the question still arises, what was the direction of the current during the hight of glaciation? We have abundant evidence to prove that, during the hight of glaciation, the main current was a southeasterly one. On the Long Lake quadrangle in the midst of the Adirondacks Professor Cushing has recorded a number of stfiae all of which point toward the southwest. Over the region south of the Adirondacks and the Mohawk valley the observations of both Brigham? and Chamberlin? show that the ice moved in a general southwesterly direction. Another strong evidence favoring the southwesterly current is the distribution of glacial boulders over the *N. Y. State Mus. Bul. 115. 1906. p. 405. * Amer. Jour. Sci. 1895. 409:216. *loc. cit. p. 365. 46 NEW YORK STATE MUSEUM region southwest of the Adirondacks. Most of the common Adiron- dack rock types are strewn over the region and they gradually diminish in number as the distance from the mountains becomes greater. This subject has been discussed in a paper by Brigham. Thus, bearing in mind all the facts, the writer is strongly of the opinion that when the ice in its southward movement struck the Adirondacks, it was divided into two currents flowing around the mountains and meeting in the Mohawk valley; that during the time of maximum glaciation there was a strong general southwesterly current, but that the border currents continued as under currents (more or less checked in velocity) ; and that after the disappearance of the ice sheet from the central Adirondacks, border currents were maintained. According to this the Port Leyden quadrangle was first invaded by a tongue of ice which flowed southeastward up the Black river valley. When the general ice sheet had here reached a thickness of several thousand feet the main current was south- westerly, but with a southeasterly under current in the valley bot- tom. The ice first melted from the highlands and left a tongue of ice in the valley which gradually melted and retreated northward. ICE EROSION Erosion of the Precambric rocks As the ice moved across the quadrangle, the preglacial rock sur- face was more or less scratched, polished and eroded. In the case of the Precambric rocks it is doubtful if the ice did any very deep cutting. Its work of erosion involved mostly the removal of masses of decayed and weathered rock material near the surface. The evi- dence is conclusive that the weathered materials were rather thoroughly scraped off the Precambrics as shown by the remarkable freshness of the rocks wherever exposed and by the smoothed and rounded character of the outcrops [see pl. 3]. The highly jointed character of these rocks no doubt greatly aided the ice in its work of erosion. Mention should be made of the great number of erratics of Precambric rock material strewn over much of the region, especially toward the south. One of these erratics measures about 17 feet high-and-27 teet across see pljie|. “Whe larger ones aac mostly of the hard, homogeneous syenite or granite. Probably the greatest amount of erosion of the Precambrics occurred along Black river between Lyons Falls and Lowville, but this matter wi!l be referred to below. =106.-Cit, Pp. 213-28. GEOLOGY OF THE PORT LEYDEN QUADRANGLE 47 Erosion of the sedimentaries Turning our attention to the sedimentaries, we find that ice erosion was much more effective upon them. In fact the writer believes that in the Black river valley we have one of the best examples of ice erosion in northern New York. One factor favoring the ice work here was the comparative softness and highly jointed char- acter of the rocks, while another factor was their position with ref- erence to the ice current. The figure on page 48 shows the profile and geologic structure across the Black river valley 2% miles north of Lyons Falls. One of the striking features is the terraced character of the sedimentar- ies, particularly from Port Leyden northward [see topographic map|. Along the river course there is a slight notch in the Pre- cambrics and just west of this, on the northern part of the Port Leyden sheet, there is a steep slope rising 300 feet above the Pre- cambrics. The formations outcropping on this slope are shown in the section. Resting upon the Precambrics are several feet of weak sandstones which are followed by the sandy limestones of the Pa- melia; then come the hard Lowville and Black River limestones ; while the summit is capped by hard, crystalline limestones. The streams passing over this slope are characterized by gorges with waterfalls and rapids. From the summit of this slope and extend- ing for several miles westward there is a well defined terrace developed upon the limestone. Rising from the western side of the above named terrace there is a second slope higher and much steeper than the first. The rise is commonly about 450 feet within 4% mile. The soft Utica shales outcrop at the base of this slope and they are followed by the Lorraine shales with an upward increasing sandstone content. The summit of this terrace, known as Tug hill, is more irregular and stream dissected than the limestone terrace below. All streams flowing across the steep slope of this terrace have high gradients and have cut deep, narrow gorges locally called “ gulfs.” : At first these terraces, in their present form, were thought to have been due entirely to water action, but an examination of the region shows that some other explanation must be sought. The steep fronts of the terraces are certainly young topographic features, which precludes the possibility of their having been formed during the long preglacial period of erosion in this ancient region. On the other hand, Black river has done very little work of erosion, between Lyons Falls and Lowville, in postglacial times as proved by the fact MUSEUM NEW YORK STATE 48 ‘[PULPN}IBUO]T 944 SOUII] Bg B[VOS [BOIJIBA ‘*sJUIUIIPEs d1OZOeTeg 9Y4 JO JeJOzIBYO peseviie} 944 puv sjisodep eyjep ey} Fo uorIscd 9y} SulMoyYs ‘sey SUOA7T JO YAIOU Sa $2 B[SuUeIPeNb UspAeT jJ10g ey} SSO1De UOT}OAS JseM-JsVq S “Og OIYBWVOAYd eo lait ay (C3ITVIONOD) OINDZOIIVd SINCE SO Te eae AMV iss st AMOT VI WV fee 093MS0 fon] NOLNAYL FF y~] VLT3SQ INIIOLSIAId PST Cale — GEOLOGY OF THE PORT LEYDEN QUADRANGLE A9 that the stream has not yet cut its way through the alluvium and reworked drift filling the valley bottom, and also because glacial striae and kames near the river level have not been disturbed. Thus also the slight trench cut into the Precambrics along here could not have been postglacial in origin. There is still the possibility that glacial waters might have de- veloped the terraces, but there is no evidence of any such vigorous water action especially along the higher part of the limestone ter- race where records would surely be left. Even if a large stream had flowed along the ice edge and under the steep front of Tug hill its gradient would have been too low to be compatible with much cut- ting power. No doubt there was movement of water along the wan- ing Black river ice lobe, but the only current of any importance was a northerly one between the eastern edge of the limestone terrace: and the ice margin [see below]. ‘The limestones here are some- what water-worn, but the stream was about 200 feet below the top of the terrace and thus clearly could not have done the work of erosion over the whole terrace. Also the presence of glacial striae on the terrace shows that no great amount of erosion could have taken place there since the ice retreat. It seems certain that the lowermost Paleozoic layers must have extended farther eastward, by overlap on the Precambrics, im- mediately preceding the glacial period. This means that Black river was some distance farther eastward and that the western tributaries from Tug hill entered it with lower gradients. As above shown, the lowest sedimentary beds could not have been cut back to form the steep slope now facing Black river in pre- or postglacial times nor were they cut back by glacial waters. Evidently they were cut back by the ice to develop the steep slope. This allowed Black river to shift westward to its present position. Thus the slight trench in the Precambrics here could not have been preglacial. As already shown it is clearly not postglacial and apparently it was formed by ice cutting. The concave character of this inner por- tion of the valley is brought out in the figure and strongly suggests ice work. The fact should also be considered that we are here dealing with unaltered sedimentaries, with slightly upturned edges, resting upon a rather smooth surface of igneous and metamorphic rocks, and that | the lowest sediments are weak sandstones and sandy limestones, which greatly favored the stripping off power of the ice. Robert 50 NEW YORK STATE MUSEUM Bell? has noted similar conditions in Canada and he says that when the ice sheet moved from the crystallines against the edges of the unaltered sedimentaries “ great erosion has always taken place and valleys and basins are formed whose width depends upon the angle of dip and the softness of the strata which have been scooped out.’ The strata are presented in the most favorable attitude for abrasion. The wearing down would go on till the resisting rock front had attained a hight and weight sufficient to counterbalance those of the glacier.” In the Black river valley the ice moved from the crystal- lines against the slightly upturned edges of the sediments. — In much the same way the soft shales were stripped off the sur- face of the hard limestones to form the broad terrace and the steep front of Tug hill. Such a stripping off of the shales occurred, but to a less extent, over the southern part of the Port Leyden quad- rangle and the western part of the Remsen quadrangle. The maxi- mum thickness of shale thus removed was probably several hun- dred feet, but not over a wide area. The total amount of shale re- moved was not nearly as much as may at first sight be supposed. Then too the shales were soft and highly jointed even to a consider- able depth as may now be seen in the Whetstone gulf section. Two other factors which greatly aided the work of the ice in the Tug hill region must not be overlooked. One of these is the fact that the ice moved up hill as it advanced southward along the valley and so had its cutting power increased. On reaching the divide be- tween Black river and West Canada creek the cutting power was lessened and till and other drift materials were deposited in great quantities as the ice moved down hill toward the Mohawk river. Another factor which the writer regards as important in this con- nection is the angle at which the ice current entered the Black river valley in its sweep around the Adirondacks. The greatest amount of erosion was along-the eastern side of Tug hill, and it is just here where the ice current must have struck with greatest force as it crowded into the valley. In harmony with this idea is the fact that the glacial striae near Martinsburg bear more toward the south than does the steep front of Tug hill. It may be fairly asked, what became of the materials thus re- moved? ‘The very resistent Precambrics ought to be present in considerable force somewhere in the region as erratics and this is the case southward especially in the townships of Boonville and Remsen where vast numbers of such erratics may be seen. Shale 1Geol. Soc. Am. Bul. 1890. 1:206. a). ee eS ee aS se A Plate 10 W. J. Mitler, photo | Looking down Moose river from Goulds Mill. The river here, | between Goulds Mill and Lyons Falls, flows through a drift-filled | channel. | GEOLOGY OF THE PORT -LEYDEN QUADRANGLE 5. and limestone are also present in great abundance in the till and other drift of the Remsen quadrangle. However, much of the shale must have been ground up and carried away by glacial waters. Glacial sand plains or terraces A remarkable development of glacial sand plains or terraces is to be found within the Port Leyden quadrangle. Here, on the east side of the river, most of the region is occupied by these terraces, which taken together may be looked upon as a single great terrace with steep front facing Black river [see fig. 5]. On the Port Ley- den sheet alone they cover fully 75 square miles and continue both northward and southward from this area. They are clearly shown upon the topographic map. The sands and gravels of these terraces show a depth of from 200 to 250 feet along the western edge, and there is a gradual thinning out to disappearance several miles east- ward. _ Except in a few cases the flat-topped surfaces are practically desti- tute of large boulders. A characteristic feature is the presence of pitlike or kettlelike depressions over the surfaces [see map]. These depressions are of various sizes and shapes and are sometimes occu- pied by lakes or ponds, as for example Brantingham, Little Otter and Catspaw lakes and Sand pond. They are often very steep- sided and range in depth from a few feet to 50 or 60 feet. . The terraces are dissected by many streams so that enough good sections are exposed to make it certain that the materials are crudely strati- fied and cross-bedded, and occasionally interstratified with clay, thus proying that they were water laid. The western margin of this great terrace is distinctly lobate in character and is strongly sug- gestive of delta origin as for example in the southeastern part of the quadrangle. Another very notable feature is the concordance of altitudes at about the same distance back from the margin. The altitudes vary from about 1150 to 1260 feet, the higher altitudes being on the east, thus giving a gradual slope of the terrace surface toward Black river. A study of the character and distribution of these terraces as well as their relation to the other drift deposits, leaves no doubt as to their origin as delta deposits in a marginal lake along the waning ice tongue during its retreat from the Black river valley. The im- mense amount of material thus deposited was readily obtained bv the streams, especially Black and Moose rivers and Otter creek, as they emerged from the newly drift-strewn Adirondack highlands. 52 NEW YORK STATE MUSEUM That they were deposited along the ice margin is clearly established by the presence of kames and large drift boulders along the western edge which prove an ice contact front here. The gradual down- ward slope of the sand plains toward the west is to be accounted for by the gradual lowering of the marginal lake level as the ice retreated. | The depressions within the sand plains may be explained in either one of two ways. They may have been due to isolation of ice masses from the ice margin (possibly sometimes as icebergs) which were partially or completely buried under the delta sand to be melted later thus causing the development of the depressions, or they may have been due to unequal deposition of the delta materials whereby some places were not brought up to the general level. The depth, steepness of sides and irregular shapes of the depressions cause the writer to favor the first view to account for most of them. Kames IKKames, which are hillocks of crudely stratified materials de- posited at the ice edge, are rather abundantly represented except on the east side over the sand plain area. There is no group of large kames such as those of Park and Sperry hills within the Boonville quadrangle, or like those of the Remsen quadrangle described in a former report. Probably the best example of a single kame 1s the one 34 of a mile southeast-south of Greig. It is remarkable for its steepness and symmetry of form and shows a hight of at least 150 feet. Many kames are located along the steep western front of the great sand terrace above described, especially from Lyons Falls northward. Other good examples may be found from south of Port Leyden to north of Lyons Falls along the railroad; south and west of Talcottville; along the road from Turin to-Houseville; south and east of Martinsburg; and even on the highland southwest of Mohawk hill. Frequently, as in the locality last mentioned, there are long low ridges of stratified materials called eskers associated with the kames. : No doubt kames were also formed over the region now covered by the sand plains, but as the ice gradually retreated from the valley the kames formed along the ice edge were buried under the deep delta deposits. Only those along the western margin of the great delta deposit were left uncovered. Partially buried kames in the midst of a sand plain are finely exhibited around Forestport on the Remsen quadrangle. The sands are there comparatively Plate 11 y fry Sy W. J. Miller, miote An erratic or glacial boulder of syenite in the bed of Black river 2 miles northeast of Boonville. The boulder is about 27 feet across and 17 feet high and rests upon Black River limestone. nv, GEOLOGY OF THE PORT LEYDEN QUADRANGLE 53 thin and after the formation of the kames and withdrawal of the ice edge, the delta sands were deposited around them but not with sufficient depth to cover them. Erratics Like the kames, glacial boulders or erratics are scattered over all parts of the quadrangle except the typical sand plains. Their absence from the sand plain belt is to be explained iff much the Same way as the absence of the kames, that is after the boulders were dropped by the melting ice they were covered by the delta deposits so that they are scarcely ever seen except along the larger stream courses where they have again been exposed by erosion. A good many are present along the western front of the delta terrace particularly in the vicinity of Greig. They are also strewn over the Paleozoic rock area, even on the high land of Tug and Mohawk hills. Mimeettavics ate mostly from the hard, resistant Precambric . formations and, as above pointed out, their presence on the high western portion of the quadrangle strongly argues for a southerly or southwesterly ice current at one time. The largest erratic ob- served by the writer is one of quartzose syenite, already referred to, which rests upon the Black River limestone about 2 miles north- east of Boonville. This boulder measures about 27 feet across and 17 feet high. Another large one may be seen in the field about 34 of a mile east-northeast of Denley station. Glacial lakes A very interesting and extensive glacial lake occupied all of the sand-flat country on the east side of Black river between Forest- port and Lowville. It also extended somewhat west of Black river in the vicinity of Boonville, and to an unknown distance north of Lowville. The former presence of this large lake is conclusively shown by the great development of unquestioned delta deposits, associated with clays, and the remarkably concordant altitudes of the sand plains [see above]. These waters were impounded by the waning lobe of ice in the Black river valley. The kames and drift boulders along the western edge of the great delta deposit show an ice contact from there; also the absence of delta deposits on the west side of the valley, under Tug hill, shows that the lake did not extend that far west. Again the failure of any delta deposits to reach out to or across the valley bottom also argues for ice occu- 54 NEW YORK STATE MUSEUM pancy of the deepest part of the valley during the existence of the large lake. In his description of the deposits along the Connecticut river, Gulliver has noted similar features and argues that those deposits must have formed before the ice had completely melted from the valley.? The highest water level in this lake was apparently something over 1300 feet at which time an outlet probably crossed the Black river-West Canada creek divide? near Honnedaga (Remsen sheet) and flowed southward toward Trenton Falls. Possibly the extensive sand deposits near the latter place were formed by this outlet, although West Canada creek may have contributed to their forma- tion. Further retreat of the ice lobe down the Black river valley certainly opened an outlet southwestward past Boonville and down Lansing kill toward Rome causing deposition of the great delta deposits north of the latter place. This delta no doubt formed in Lake Iroquois or rather its broad outlet in the Mohawk valley. This outlet from the glacial lake affords a fine example of a “through valley’ to use the term suggested by Davis. The pre- glacial divide was doubtless near Hurlbutville as shown by the widening of the channel both northward and southward from that place; by the existence there of a deep inner gorge; by the ag- graded stream bottom north of Hurlbutville; by the fact that the present stream could not have cut the deep narrow channel north of Hurlbutville and by the right elevation of an outlet there. The lake stood at approximately the 1250 foot level when it started over this divide and it cut down the divide rapidly until the 1140 foot level in the lake was reached. By this time the ice tongue had so far melted as to allow an escape of the water northerly and north- westerly along the west side of the. ice tongue and into Lake Iroquois near Watertown. These north moving waters have left the limestones just west of the river more or less waterworn and possibly some of the minor terraces were formed by them. Another lower and very distinct lake level was a little below 800 feet and caused by still further ice retreat to allow an accumulation of water back of a barrier at Carthage. The river is still engaged in cutting through this barrier. This lake extended southward to Lyons Falls where it was very narrow. Between Lyons Falls and Carthage the river now shows a very low gradient and the winding 1 Am. Geol. Soc. Proc. 1907. 18:640. >The rather recent land movements in the region are not considered. Thus the elevations given are comparative only, but they. are not far from the actual lake levels which were doubtless lower. GEOLOGY OF THE PORT LEYDEN QUADRANGLE 55 a stream is developing terraces through the old lake deposits of the valley bottom. Drainage Black river and its tributaries. From Hawkinsville to opposite Denley, Black river is certainly out of its preglacial channel as shown by the gorge cut into the limestones. Its former course was probably about 2 miles eastward along the Paleozoic-Precambric boundary. Between Denley and Port Leyden it is practically in its old channel. Thence to east of Lowville the stream is somewhat west of the preglacial course due to the westward shifting of the Paleozoic-Precambric boundary by erosion during glacial times. It Paeweiri! if any Of the tributaries of Black river, which cut through the delta deposits and into the Precambrics, follow their old channels because they have been superimposed upon the Pre- cambric surface. Thus Moose river has cut through the deep sands and is now engaged in eroding a channel, with gorges and water- falls, into the Precambrics. Origin of the “gulfs.” The deep gorges which have been cut through the steep eastern front of Tug hill, by tributaries of Black river, are locally known as “ gulfs.” The chief gorges are occu- pied by Mill, House, Whetstone and Atwater creeks and Roaring brook. Whetstone gulf which is perhaps the most interesting, is about 2 miles long and shows a depth of 300 feet [see pl. 9]. Its walls are very steep sided to almost vertical, especially in the upper end (narrows) where there is just room enough for the stream at the bottom and where erosion is now proceeding most rapidly.: A section showing something like 700 feet of Lorraine and Utica shales is finely exposed in this gorge. The stream emerges from the “gulf” upon the broad limestone terrace. During glacial times the shales were eroded back over the lime- stone for a considerable distance, and this caused the development of the steep eastern front of Tug hill. After the disappearance of the ice from the region, all of the east bound streams from Tug hill rushed over this steep slope and began to erode notches into its summit. These notches were rapidly deepened in the soft shales to develop the “ gulfs,’”’ whose heads have since been cut back to their present positions. South of Tug hill the “ gulfs” are not so well developed because the shales, with their preglacial channels, were not cut back by erosion to such a great extent. 56 NEW YORK STATE MUSEUM ECONOMIC PRODUCTS > ~ Soils The principal industry of the region is farming and the success of that industry here, as elsewhere, depends. not only upon the character and energy of the people, but also, to a large extent upon the nature of the soil.. The Port Leyden quadrangle affords us a fine'example of the dependence of agriculture upon the geologic formations. From the standpoint of fertility of soil, Black river divides the district into two portions which present a remarkable contrast. Eastward from the river the territory is mostly covered with deep sands and gravels which are generally unproductive. Occasionally along the stream bottoms or where some clay is mixed with the sand, the soil is of fairly good quality. The potato crop is best suited to’ this sandy.soil: -There are many deserted garusemen this side of the river and apparently this section was most pros- perous when lumbering was the chief occupation of the people and farming a secondary matter. On the west side of the river where the geologic formations are chiefly limestones and shales, and where sands and gravels are sparingly present, there is a prosperous farming community. Here the surface is mostly strewn with glacial debris which is largely composed of ground up shale, sandstone, and more or less lime- stone, which is thus a rich and easily worked soil. Building stone Building stone of fine quality occurs in immense quantities within the map limits. The rocks most quarried for this purpose are the limestones of the Pamelia, Lowville and Black River formations, but especially the Lowville. Many large quarries have been opened up in these formations, the principal ones being located on the geologic map. Such stone was used in building the numerous locks of the Black river canal and then later by the railroad for bridge abutments. It now has a considerable local use, especially for foundations. The highly jointed and stratified character of the Lowville and Pamelia beds cause it to be readily accessible in layers of almost any desired thickness up to about 2 feet. The Lowville is a bluish gray, very fine grained, pure limestone, while the Pamelia is usually a whitish gray to pink, more or less sandy and impure limestone. The gray Black River limestone quarries out as GEOLOGY OF THE PORT LEYDEN QUADRANGLE By a more massive stone. The most extensive quarries are between the mouth of Sugar river and Denley station. Other good building stone is found in the Trenton limestone. especially the upper portion. This rock is gray, coarse grained, crystalline, and pretty pure and may be quarried in layers from a few inches to a foot thick. The stone is much used locally and was formerly burnt in great quantities for the production of lime. The chief quarries are at Talcottville, Turin and Martinsburg. The sandstones of the upper Lorraine are strewn over the highlands on the west and are of considerable local use. Of the Precambric rocks, the syenite is an excellent building mi@ertals If is a very hard, greenish to reddish, rather granitic syenite which takes a high polish. The expense of quarrying and transportation have almost entirely prevented its exploitation. A quarry from which syenite of fine quality has been taken is located about a mile east of Denley station. Road materials - Most of the Precambric rocks, but especially the syenite, because of its great durability, when crushed would yield excellent road materials. Most of the stone now used for road work comes from the Lowville and upper Trenton limestones because this stone 1s cheaply quarried and crushed and is fairly durable. Sand and gravel As above explained much of the country east of the river is deeply covered with sand and gravel, often of good quality for ail sorts of uses. The increasing demand for such materials will, in the future, doubtless cause the exploitation of these immense deposits. Iron ore In the above descriptions of the Precambric rocks, magnetite, in small grains, is seen to be very commonly present. Many times patches of magnetite 1 or 2 inches across have been observed in the mixed gneisses and in the more acid phases of the syenite and they have every appearance of being segregation masses. An ore body several feet across has been found on the Murtaugh farm 2 miles east of Glenfield. It is magnetite mixed with much pyrite and is closely associated with pegmatitic material in the granitic syenite. The pegmatite and ore seem to grade into the country rock and probably represent a segregation mass. 58 NEW YORK STATE MUSEUM The most interesting and important magnetite deposits occur in the village of Port Leyden and on the west side of the river below the bridge. Many years ago several attempts were made to mine the ore here. An ore pit, now filled with water, was run down some 50 or 60 feet and a furnace was erected, but the mine was _never a paying proposition. Ore was later brought to the furnace from other places. The ore is magnetite associated with much iron ‘ pyrites and often with quartz. } — =f Jn. 7 * rs = A =<, Se Be . “ . <= . ‘ . . =" P <) J ‘ - e E : 1 v 2 ELIZABETHTOWN AND PORT HENRY QUADRANGLES 21 Chapter 3 GENERAL GEOLOGY Grenville series Introduction. Far the greater part of the area consists of the ancient Precambric rocks, a very complex group, which, however, can be deciphered into several recognizable and distinguishable com- ponents. Along the shores of Lake Champlain in embayments or projections extending from northeast to southwest up into the val- leys between the ranges which come down to the lake, are found the Paleozoic sediments, beginning with the Potsdam sandstone and ending with the Utica slate. One dike of igneous rock has been found, which cuts the Paleozoic strata. Some miles west of the Champlain valley and separated from the main Paleozoic exposures, one outlier of Potsdam has been discovered and there are indica- tions of a second, 1% miles west of Elizabethtown, although only loose float has been seen. The Precambric rocks are usually metamorphosed and are in instances much changed from their original condition. The Paleozoics are not greatly recrystallized and are much contrasted with the older formations. The two can well be treated separately and, as here, by different writers. Precambric formations in general. The Precambric complex is separable into an older sedimentary portion and a later igneous portion. The sediments occupy far the lesser area, and must be but a fragment of what was originally a widespread series, which has been invaded, broken up and metamorphosed by the eruptives. In fact one can only gain a comprehensive grasp of the total geology by picturing a sedimentary area penetrated and overwhelmed by a vast igneous outbreak. We have, however, only the deep seated rocks. There is reason for believing that the overlying volcanics which probably accompanied them were all worn away long before the Potsdam epoch opened. With them went also undoubtedly a vast amount of the ancient sediments. The grounds for this belief are, the relatively small amount of the sediments now remaining ; the deep seated character of the eruptives; and the need of assum- ing some load now gone, beneath which these igneous rocks could crystallize in their present coarseness of grain. It is also conceive- able as-an alternative that the igneous rocks were altogether intrusive, and that there were enough sediments over them to supply the pressure and the conditions of slow cooling. We can only contrast the two possibilities since no actual trace of one remains more than of the other. 22 NEW YORK STATE MUSEUM The Precambric rocks are classifiable in order of age from the latest to the oldest as follows: ; Lhe unmetamorphosed basaltic dikes The eruptive complex of more or less metamorphosed granites, anorthosites, syenites, gabbros and intermcdiate types. The Grenville series of limestones, ophicaicites, schists, and sedi- mentary gneisses Grenville series. The name Grenvilie was originally given by Logan to a series of rocks in all respects similar to the one here under discussion and developed in the township of Grenville, On- tario. Ebenezer Emmons in his early work in the Adirondack area ~ spoke of them as primary, and, under this head, placed the lime- stones (called primitive limestone) and the serpentine with the ig- neous rocks, while the gneiss was classed with the stratified. It is one of the curious instances of the changes in geological thought, that 60 years later these views are exactly transposed. In later years the wise custom has developed of applying geographical names to formations and for this reason the term Grenville is here adopted. It is true that a gap intervenes between the Adirondacks and the Canadian exposures in Quebec and Ontario, and that this gap is covered by the Paleozoics, but the similarity of the old sedi- ments in both areas 1s so great, that there seems little doubt that they are equivalents. The International committee, which visited both regions in 1906 and submitted a report on the correlation of the two were at least sufficiently impressed with the similarity to recommend the uniform use of Grenville. The Grenville strata are widespread in the Adirondacks, scarcely a quadrangle being without them. On the Port Henry sheet and along Lake Champlain just north of Port Henry is one of the best exposures in the eastern mountains, but they also appear at a number of other localities in the area here described. The most prominent and easily recognized of the members is a white crystalline limestone, very coarse grained and seldom pure or uniform over any great width. It is marked by small inclusions of pyroxene, graphite and less common individual minerals and by larger streaks and pegmatitic aggregates of coarse quartz, feld- spar, hornblende, biotite, tourmalin, titanite, pyrrhotite and scapo- lite. Where the limestone has been quarried for fluxing purposes in the iron furnaces, as has been the case near Port Henry, large dumps of the rejected silicates have accumulated, and now afford 1 Jour. Geol. 1907. 15 :IQI. SOUIUL OITYSIOF[IG Ive + ouoj}SoUN] UL YsIyos apustquioy Mou ‘ayIp poaqney ELIZABETHTOWN AND PORT HENRY QUADRANGLES © 23 interesting material for the mineralogist. This limestone is a fairly pure calcite. Overlying the limestone stratum at Port Henry there is another of ophicalcite, or of limestone speckled with included masses of serpentine. This stone has been the object of quarrying and, fur- nishing as it does, a variety having a white base with light and dark green mottlings distributed through it, has commanded some attention as an ornamental stone under the name of verde antique, or Moriah marble. The serpentine is believed to be due to the hydration and alteration of original diopside, whose unchanged cores may be sometimes detected within the mass of serpentine.’ Wiis is practically the same rock as that which furnished. the Fozoon canadense, to the early observers, but no good specimens of this exploded organism have been discovered. A very characteristic minor associate of the limestones is a lemon-yellow quartzite or quartz-schist, with more or less dissem- inated graphite. The yellow color is doubtless due to decomposing pyrites and the rock will often yield the astringent taste of iron sulphate. Black and coarsely crystalline hornblende schist is also a common associate of the limestone but in relatively small amounts. It may contain large red garnets. The observer is often puzzled whether to interpret this rock as an altered intrusive mass of gabbro or as a metamorphosed sediment. There are probably cases of both. The remarkably regular masses which cut across the exposures, and have a uniform and moderate thickness suggest an intrusive origin most strongly of all. Over the Pease quarry just north of Port Henry there is such a black band, and one courses through another quarry in Pilfershire, southeast of Mineville. Along the Delaware and Hudson railway tracks on the lake shore north of Port Henry where there is an irruptive contact of gabbro and basic syenite and limestone one can see the igneous rock. tongu- ing out into the limestone and apparently pinched off at times by the dynamic disturbances. While it is entirely possible that the hornblendic rocks have been derived from aluminous bands in the original sediment, which might yield greater or less amounts of hornblende, yet we are dealing with a district in which are numer- ous intrusions of gabbro and basic syenite and where apophyses are abundant. The marked plasticity of the limestone under pressure 1 Merrill, G. P. Notes on the Serpentinous Rocks from Essex Co., eee ete SO eeeNat Mus. Proc. 1890. 12:595—600. 24 NEW ‘YORK STATE: MUSEURL™ tends greatly to disguise the relationship and to render a demon- stration difficult. lgneous phenomena and their expiring effects must have been very general and have probably occasioned wide- spread recrystallization. Undoubtedly tney have set in migration many heated solutions. The limestone becomes at times extremely small in amount and may be represented by little more than calcareous streaks amid more siliceous rocks, such as mica schist and quartzite bands. ‘he whole may be folded in.a most remarkable way. The more re- sistant silicates having been involved in a plastic medium like calcite have been bent into shapes that seem almost beyond the power of brittle minerals to assume. The presence, however, ot the lime- stone is indicated by the pitted and cavernous weathering. Mica schist or schistose gneisses are known in several localities which also represent the sedimentary series. The rocks are thinly laminated and are much more abundantly provided with biotite than are the eruptive gneisses. The banding runs regularly for greater distances and reproduces the persistent bedding of sediments rather than the sheared and dragged individual minerals of the eruptives. Besides the more schistose gneisses there are others less thinly or regularly banded and yet not corresponding exactly to any of the well defined eruptive rocks. Where they display sharp contrasts of light and dark bands which are persiscent over distances of sev- eral feet or more and which are dithcult to explain except on the basis of the contrasts in composition which might arise 1n sedimen- tation, the writer’s disposition has been to group them with the sedimentary types. It is realized that eruptive rocks themselves do display marked banding and gneissoid structures which are due to magmatic differentiation! but yet in open questions like those presented in the Adirondacks, as a matter of opinion the writer leans rather to the sedimentary interpretation especially when the rocks are associated with undoubted sediments. | Some complication arises because of the abundance of pegmatitic matter even on a small scale. Injected gneisses are not unknown and inasmuch as such quartzites as can be recognized in the region are so thoroughly recrystallized as to simulate vein quartz or pegmatitic quartz, lenticular masses of this character may at times give rise to the suspicion of old sandstones. Well defined quartzites are, however, much less in evidence in the two quad- rangles under discussion than in several to the south. en al ~ 1As very clearly shown by Sir Archibald Geikie and J. J. H. Teall for the gabbros of Skye. Geol. Soc. Lond. Quar. Jour. 1894. 50:645. Folded interbedded schist in Grenville limestone, along the Delaware & Hudson Railroad, north of Port Henry ou : 4 ; 4 poroyyeom pur soqvoqqis JO Syvat]S YUM posieyo ‘AlueP{ 3JOg JO YZIoU ‘peospIey UOspryT WW oiemejoqd suoje Iuoj}sowly I]tAuat+) ELIZABETHTOWN AND PORT: HENRY QUADRANGLES 25 In the Paradox Lake quadrangle which lies next south of the Elizabethtown and also in the Whitehall, which is southeast of the Paradox Lake, there are extensive developments of a richly gar- netiferous, green gneiss, often with much sillimanite. None of this has been observed in the Elizabethtown-Port Henry area. Its original is believed to be a somewhat calcareous shale and it is characteristically associated with the graphitic schists or quartzites which are the commercial sources of graphite. Its absence would argue some change in the character of the Grenville sedimentation to the north, presumably to more purely siliceous or feldspathic materials, whose metamorphic derivatives lack both the lime and the carbonaceous components. In addition to the above, which may be considered fairly well de- fined sedimentary types, there are great masses of decidedly gneiss- oid rocks, usually granitic or at least quartz-bearing in composition, with hornblende and augite as the common dark silicates and with coarse crystallization. They are well shown in the ridge of Bald eae ald they are extremely difficult to interpret. The writer’s disposition is, on account of mineralogical composition and associa- tions to regard them as igneous in character. They are placed with the syenite series as an acidic extreme. It is realized that another observer might develop a strong argument for their sedimentary characters. It is felt that the best course is to fully and fairly state both cases hereafter. | Chapter 4 GENERAL GEOLOGY (continucd) Metamorphosed eruptives This group is contrasted with the next one of the unmetamor- phosed basaltic dikes, because the latter are obviously much later and because they followed the period of metamorphism and crush- ing, presumably also of extensive erosion, to which the former were unquestionably subjected. At the same time it is believed that the dikes are older than the Potsdam and that they belong to an en- tirely different set from the ones which penetrate the Paleozoic sediments! in adjacent areas. The older eruptives with the possible exception of some ex- posures of the basic gabbros constitute extended and huge masses 1See in this connection the following paper by H. P. Cushing who was the first to show the distinction between the two groups. On the Existence of Precambrian and Postordovician Trap Dikes in the Adiron- dacks. N. Y. Acad. Sci. Trans. 1896. 15:248. 26 NEW YORK STATE MUSEUM of plutonic rocks. They are batholiths or great, deep seated volume, of irregular shape. The included fragmen*s of older rocks which have from time to time been detected demonstrate their intrusive nature. These and the nature of the intrusive con- tacts give such clues to their relative ages as can be obtained. The original outlines of the intrusions, that is, the evidence as to whether thcy ever assumed the laccolithic or other definite shapes, have been rendered wellnigh undecipherable by faulting and erosion. Granites and related types There are several areas to which this name has been distinctively applied. While they are described before the anorthosites and other eruptives their relations to the latter are obscure. In general they are believed to be older, but there is little ground for this belief other than their intimate association with the Grenville. Their dis- tinction from the acidic members of the syenite series is, moreover, not in all cases clear; and the possibilities of the occurrence of shales and feldspathic sandstones in the Grenville, which might yield, upon extreme metamorphism granitic gneisses, have not been overlooked. Nevertheless both in the field and in the laboratory the occurrences here colored and described as granites, have impressed themselves as sufficiently distinctive to justify the procedure. The largest area is in the southeastern corner of Bulwagga moun- tain. A biotite granite is very abundant all through this portion of the sheet, so much so as to be the predominant rock. While it may not be the exclusive member, the variations can not well be shown in colors. Excellent exposures appear near the iron bridge at the headwaters of Grove brook. In their section microcline is the most abundant mineral while quartz and biotite practically com- plete the slide. This combination is in contrast with the mineralogy of the other groups of eruptives. Both microcline and biotite are seldom seen in the latter, and the inference is natura] that when they predominate we are dealing with a separate intrusive. In the western portion of the area colored green, red granitic rocks have been observed, which reveal under the microscope no dark silicates, but which have only finely striated plagioclase and quartz. A few decomposition products, perhaps from dark sili- cates, and a few tiny zircons complete the slide. Throughout this granitic area much pegmatite is present and the granites are often cut by it. About 3 miles north of Port Henry another area of small dimen- ¢ > 3 se ELIZABETHTOWN AND PORT HENRY QUADRANGLES 27 sions appears on the east and west road. To the observer in the field this appears like a pronounced intrusive granite, sheared more or less into a gneiss, but different from both the syenite series and the Grenville. The microscope reveals quartz, microcline, micro- perthite and hornblende. It is, therefore, not so sharply contrasted with the acidic members of the syenite series as is the Bulwagga - occurrence, in that it has microperthite and hornblende, but it has microcline and in the ledges it looks unlike the syenite series. There are two other small areas colored for granite, and lying southwest of Westport. Both of these are coarse gneisses, reddish -in color, with their quartz and feldspar in little, interleaved lenses, up to an inch in length. No microscopic slides have been prepared and the rock might perhaps be justifiably placed with the syenite series. In the field it was believed to be different. Besides the occurrences actually colored, there are one or two others deserving mention. In the gorge of Mill brook, just north ot Pott Henry, and a short distance above its mouth, there is a faa or wiite granitic rock, several hundred feet thick, in the midst of the Grenville limestones. It is obviously much crushed, is dense, white and granitic in aspect. Under the microscope its components are microperthite, microperthitic microcline, quartz, plagioclase, biotite, garnet and zircon. It is difficult to decide whether this is an intrusive granite or an altered sediment, but the former is the more probable. A mile west, up Mill brook, is the old Lee mine; its walls are a red granitic rock now strongly gneissoid. Much the same rock appears in the walls of the old Essex county ore bed in the northern slope of Bulwagga mountain, but all these last three have been colored in as Grenville. Again in the ridge, an eighth of a mile north of the east end of Crowfoot pond, granitic gneisses again ap- pear, different from the run of the syenite series, but no special color has been given them. Anorthosites The anorthosites are believed to be the oldest of the eruptives. They certainly followed the sediments because of the included masses which will be later described. They preceded the Split Rock falls type because we find inclusions of them in the latter. They are believed to be older than the syenites, not from any posi- tive evidence in the area under discussion but because they have been clearly shown to be such by H. P. Cushing in the Long Lake 28 NEW YORK STATE MUSEUM quadrangle, where the writer has had the privilege of seeing the critical exposures. The syenites are essentially the same kind of rock in both localities and in default of positive evidence which may appear at any time within the present area, this relationship is assumed. The anorthosites were called by Professor Ebenezer Emmons in his extremely valuable Report on the Second District, “ hypers-. thene”’ or “labradorite rock,” but inasmuch as the hypersthene is very subordinate and as neither of these is a good rock name, the term first employed by Dr T. Sterry Hunt in Canada, is here pre- ferred, as it is generally by geologists today. The anorthosites vary from almost pure aggregates of sleet: clase crystals through variations caused by increasing amounts of a pyroxenic component. The commonest of the pyroxenes are hypersthene and green augite, the latter on the whole being perhaps more abundant than the former. More or less titaniferous mag- netite also appears. The rocks are normally very coarsely crystal- line. In the central portion of the great masses, feldspar crystals, apparently not connected with pegmatite veins may sometimes be seen as large as a man’s hand. Crystals two or three inches across. are not uncommon. Well crystallized and uncrushed specimens are rare. The entire area has been subjected to such severe pressure and granulation that the outer borders of the crystals are almost always crushed to a finely granular and whitish mass. Within this rim the bluish nuclei of the plagioclases remain. When shearing and dragging has been added the nuclei yield augen-gneisses of the most typical and instructive kinds. The crushing may go so far as to destroy all nuclei and leave a whitish or greenish pulp of secondary products. THis is closely akin to saussurite. When weathering is added the rocks are often extremely white on ex- posed surfaces, appearing almost as 1f whitewashed. The plagioclase crystals sometimes assume elongated forms and suggest a coarse diabasic texture when there is sufficient of the dark silicates to bring this out. Rarely the plagioclase exhibits the characteristic irridescence of certain labradorites. It has not been noted in this quadrangle but in the Mt Marcy group it is not un- common in the beds of brooks, where either from pebbles, by chance properly cut, or from the smooth bed rock the irridescence flashes out to the observer. 1Cushing, H. P. Geology of the Long Lake Quadrangle. N. Y. State Mis Bullaens: 1007-2 ap. Aat. . ELIZABETHTOWN AND PORT HENRY QUADRANGLES 29 _ The variety of the plagioclase is best shown by the chemical analysis later cited but it can also be determined in an approximate way by means of the extinction angles. Measurements of specific gravity would also be significant but they have not been used as _ the above tests were esteemed sufficient. The plagioclase lies most often just beyond the labradorite ranges of Ab, An, to Ab, An,', yet short of the bytownite of Ab, An. In the more basic varieties we find the upper limits of the by- townite series also represented. Under the microscope and when the original texture of the rock has not been crushed and destroyed, the thin sections show betweer crossed nicols the characteristic twinning of the plagioclases in a remarkable degree of perfection. For purposes of instruction few rocks are so well adapted for illustrating these phenomena. At times the bands cross the crystals with mathematical regularity and perfection; again they interpenetrate and pinch out like interlocked fingers and hands. Even with low powers the plagioclase reveals the very minute dusty inclusions, which in somewhat sparse ar- rangement are distributed throughout the clear mineral. With high powers the dust is seen to be in largest part an opaque to dark brown mineral, in prismatic or tabular form according to the orien- tation and doubtless ilmenite. Rarer pale green fragments are probably diopside and spinel. The inclusions may be strung out in lines parallel to the main twinning. They are never abundant enough to affect the transparency of the slide in any appreciable degree and in this respect they are inferior in amount to those ir the basic gabbros to be later described. 1JTn the algebraic designation of the plagioclases, they are considered combinations of the albite molecule, Nas.O, AlsO:, 6SiO., written Ab and the anorthite CaO, AlO:, 2SiO2, written An. The following varie- ties are recognized by students of rocks. Albite Ab: Ano through Abs Ani Oligoclase Abs An; through Abs Ani Andesine Ab; An» through Ab, Ans; Labradorite Ab: An; through Ab; An, Bytownite Ab: An; through Abi Ang Anorthite Ab; An; through Abo An: Although the above is the assignment of species generally given in the textbooks it is not a good one, since there are uncovered gaps between each group. Ab, An; for example is not provided for. It should read Albite Ab: Ans to Abs An;; Oligoclase Abs An: to Ab. Ani; Andesine Ab: An; to Ab, Ans; Labradorite Abs Ans to Ab: Anz; Bytownite Ab; Am to Ab: Ane: Anorthite Ab; Ans to Abo Ani. 30 NEW YORK STATE MUSEUM Many years ago the late George W. Hawes? noticed in slides of these rocks some feldspars which failed to afford the twinning stria- tions yet which he suspected of being plagioclase. Analytical tests demonstrated that they were. The same untwinned character may reappear so that the observer must be on his guard, but it is also true that a chance section parallel to the twinning plane would also be without the striations. The analyses demonstrate the presence of potash quite without exception. The extreme rarity of biotite in the localities where the specimens taken for analysis were collected make it practically certain that the potash is in the orthoclase molecule and that this feldspar is in the rocks up to 5 per cent or over. It would also yield untwinned feldspar, which could only be distinguished from plagioclase by refined optical tests. The analyses prove that quartz is at times present in amounts even reaching 8 per cent. The observer would need to exercise care not to overlook this mineral, yet despite the rather large per-. centage indicated by the recasting of the analyses it is rare to detect it in the slides. It is possible that it may be separated in part during the process of saussuritization, and be so finely divided in this indefinite, cloudy mass as to escape notice. Microscopic study has shown that the commonest and most widely distributed pyroxenic component is a pale green variety, no doubt near diopside 1f not actually this molecule. The relatively high percentage of lime in the analyses is sufficient to more than satisfy the anorthite molecule and still leave an excess for the pyroxene, while the relatively low magnesia and iron serve to keep the hypersthene molecule somewhat in the background. Hyper- sthene is, however, abundant and widely distributed and as soon as the percentages of magnesia and ferrous iron rise and the anortho- sites develop larger percentages of the pyroxenic components, the hypersthene becomes prominent. In the more coarsely crystalline and pegmatitic phases the hypersthene assumes a coarseness of crystallization which combined with its easily recognized bronze lus- ter, makes it catch the eye of the observer and convince him of its presence. In the typical anorthosites the pyroxenic components are smaller in size than the feldspars and are packed in between the latter. Actual contact between the two, and especially in the ee 1 Hawes, George W. On the Determination of Feldspar in thin sec- tions of Rocks. U. S. Nat. Mus. Proc. 1882. 4 :134—-36. Ree al i ee a Li, ELIZABETHTOWN AND PORT HENRY QUADRANGLES KP! crushed and sheared varieties is often prevented by the intermedi- ate rims of garnet to which reference will be made later. Just east of Elizabethtown village in Green hill and Raven hill as well as to the north in the Ausable quadrangle, the anorthosite has much reddish brown biotite instead of the exclusive pyroxenic mineral. ‘The feldspar is also often reddish or brownish and as crushing is not pronounced the rock looks much more like a coarse mica-syenite or nephelite-syenite than like anorthosite. Yet micro- scopic investigation has invariably shown the feldspar to be plagio- clase of the normal type. The anorthosites are believed to grow more basic toward the borders. The pyroxenic component becomes more and more pro- nounced and in the end instead of forming 5 to 15 per cent of the rock, it may be 25 or over. In this respect the writer’s observa- tions are in accord with those already published by H. P. Cushing for the northwestern areas. The rock then shades into a very coarse gabbro, but the plagioclase is always the most prominent member and in the field in order to maintain the distinction be- tween the anorthosites and the basic gabbros these varieties have been called pyroxenic anorthosites. The sole difference is the increase in the bisilicates. Another mineral of almost universal occurrence in the anortho- sites is garnet. Over much of the area it is rare to find the labra- dorite in contact with the titaniferous magnetite or pyroxene. Almost always “there will be an intermediate rim of garnet which surrounds the pyroxene or iron ore like a little crown of highly 1efracting pink grains. Even in the hand specimens the rock is a very beautiful one but under the microscope where the garnets stand out in relief the effect is even more impressive. The garnet rims are not limited to the anorthosites but are found in the rocks of the next type and also in the basic gabbros under which they will be again referred to as the garnets are accompanied by other minerals. The rims rarely appear in the syenites. Larger masses of deep red garnets are also sometimes met, looking like knots in a board. They have probably recrystallized from pyroxenic material once present in the anorthosite. Chemical composition. No special analyses of the typical anor- thosite from this area have been prepared. The rock seems so simple in its mineralogy as scarcely to require them. Such analy- ses, however, as have been made of similar types either in neigh- boring or remoter localities, even including Norway, are given below, together with the percentage composition in actual minerals 22 NEW YORK STATE MUSEUM when the analyses are recast according to the methods now much in vogue and extremely useful. ; I 2 3 4 5 SiQy suc Aah aee eee Ons 5 54.62 54.47 5 3ucia 51.62 ALO se e508 3 ee 25.62 26.5 20.45 28.01 24.45 PEO sk ie ek Saat ae IS 75 TRA 75 105 das, © barter Mina? wwe a by ere OAH .56 HOGS ee Sete Se Mg @ra/ 5. fae ae tr 74 .69 63 eon CaO 5 hie ca airs eee 743 9.88 10.8 sigs 2) 9.97 Nap Ome yee eee 5.00 45 B27. 4.85 3.49 KOM eit cae eee ee 96 pe 3 .Q2 96 E27. Ono ae he eho. 45 OI 53 tr 72 PsO8 rag 15 teehee ey See eT tae eee OI iN Bot @ ae aren ree oMEGMEMCAR GH See Ugh) fee) Oe ey CY bee a ot I SDs Wiiscine dees a eee 2.66 Pa] 2672 25075 2.708 1 Chateau Richer, Quebec... T. S) Hunt. “Geol! Sur Can reo 2 Keene valley. A: R. Leeds. N. Y. State Mus, 30th) Am )Reniaems je Dp. 92. 3 Summit of Mt Marcy. A. R. Leeds. N. Y. State Mus. 30th An. Rep’t. 1878. p. 92. 4 Nain. Labrador. A. Wichmann. Zeitschr. d.d. Geol. Gesellsch. 1884. 36 :491. 5 Carnes Quarry, Altona, Clinton co. E. W. Morley for H. P. Cushing. NY: State Geoltoth An Rept, 1ool aapease: 1 The recasting of analyses was first practised by W. C. Brogger of Christiania about 1890, and has given a new significance to the chemistry and mineralogy of rocks. A simple exposition of the methods employed will be found in Kemp’s Handbook of Rocks, the calculations being pursued only so far as they give results representing actual rock-making minerals. A more elaborate method, has been developed by Messrs Cross, Iddings, Pirsson and Washington in The Quantitative Classifica- tion of the Igneous Rocks, but in its application the authors are forced because of the complicated mineralogy of many rocks to assume some minerals or molecules which, so far as we know, are not in the rocks under discussion. While the variation from the actual mineralogical composition is oftentimes not necessarily great, yet hypothetical con- ditions are unavoidably assumed. In the recasting here cinpioyed, only those mineralogical molecules are used which we have reason to believe are in the rock. While the results are not mathematically accurate and while in some cases an excess or a deficit of a component has been encountered, yet the results must be very near the truth. They have their value in that they focus attention upon the percentages of the several minerals rather than, as in chemical analyses, upon uncombined oxids. ELIZABETHTOWN AND PORT HENRY QUADRANGLES 33 I = 3 4 5 a 8.64 q.50 E62 2.4 5 Miameclase .....:... J 5.50 V8 5.004 a5e56 75 ieoclase .......... SI. 322 82.2 84.186 O1.57 61.7 MWeenige .. 1... .404 .93 1.856 .404 2eA. 1 2.58 BOY, DRO ile Mie aoe ee ae feeeess AlQ;......... Te LB ly sis Sica A Rae eae ar a stale Ren Ee aL coer tS MG ek .09 ADE A = Moen arene et TY, cee ne Sic fal oe ben de) leeks 11.75 Memncice. Hypersth... ...... ARC BeS de 4.616 222A The Light colored min.... Q9:. 234 93.97 93.39 O7 ot Wee Meni colored min.... .404. E23 6.572 3.688 25.15 Breoclase .......... Abi Any.7 Abi Anz. Ab: Anz Abi Anz. Abi Anas Meemareau Richer, Quebec. IT. S. Hunt. Geol. Sur. Can: 1863. Peieeete valley, A. R. Leeds. N. Y. State Mus. 30th An. Rep’t. 1878. i -92. : nit gremte Marcy. AR: Leeds. N.Y. State Mus. 30th An; Rep’t. fio7o. Pp: 92. A Nain. Labrador. A. Wichmann. Zeitschr. d.d. Geol. Gesellsch. 188.4. 36 :491. Seeegics Ouatty, Altona, Clinton co. E. W. Morley for H. P: Cushing. Meereestaie Geol. roth An. Rept. 1901. p. 58. In the quantitative system the first four analyses belong in class Merersaiane, order 5, Perfelic, Canadare. No. is in rang 3, Alka- Mette subtane 5 Persodic. Nos. 2, 3 and 4 are under rang 4, Meeaicic Labradorase, subrang 3, Persodic, Labradorose. No. 5 belongs in class II, Dosalane, order 5, Perfelic Germanare, rang 4, Docalcic, Hessase, subrang 3, Persodic, Hessose. Of the five analyses the first four are characteristic anorthosites but the last marks a transition to the gabbros proper. ‘The larger percentages of ferrous iron and magnesia are the indication of this and are of course the result of increasing amounts of the pyroxenic component. In recasting the analyses some important assumptions were necessary, which do not materially change the results. Thus when water was not determined in parts above and below Iio C. it was arbitrarily divided into combined and absorbed. Fe,O;, which in nos. 1 and 4 includes some FeO, was broken up so as to give magnetite. In no. 1 after the best possible combination of oxids, 1.122 Al,O, remained, and in no. 3, the SiO, failed to satisfy its natural associates by 2.40. There were probably some slight errors in determinations, for there seems no escape from the mineral- ogical compositions used. In no. 5 the most basic one and obviously well over toward the gabbros, the recast values are taken from results given by Professor Cushing and involve no kaolin. 34 NEW YORK STATE MUSEUM The results show that quartz may be expected in the moderately silicious ones although it may not be sufficiently abundant to catch the eye of the observer. The orthoclase molecule is also seldom visible in the slides. The plagioclase lies near the labradorite series but when the anorthite molecule passes the 2. ratio it approximates bytownite. The overwhelming percentage of the feldspar is ap- parent. The anorthosites are rich in the light colored minerals beyond the vast majority of eruptive rocks. To what extent the ferromagnesian molecules are to be assigned to diopside and hypersthene is not apparent. Microscopic study proves both to be present but their total is small at best. We have thus to deal with a great eruptive magma, containing little else than silica, alumina, lime and soda. Although jthe firs, to appear in a series it is probably a differentiation product from an earlier original richer in iron and magnesia. The later residual outbreaks profited by these accumulated bases which were left behind. Inclusions. In the bare ledges along Coughlin and Stevens brooks which flow eastward down the eastern buttress of Giant mountain several cases of included fragments of older rocks, un- doubtedly belonging to the Grenville series have been discovered. Figure 4 illustrates the shape and size of one. They have uni- formly a garnetiferous border marking their boundaries against LAK SS SLT ISLA ET LDS IDA ISS SIT AA Le YZ LAS STRETFORD IT YO SGAADS PREIS ILLS A Yen LS SASS ALF MOLAA IS Gf LIE TL OMS TAL. fof lame Se LL LIS GTS fe (1 11JA, Lister NIN IN TPES CAACPRIENS MAIR DOO Vaca Ae er ge Vee CNG ESN EN SAGTG LIPSENSE NIN ELIZABETHTOWN AND PORT HENRY QUADRANGLES oT. I 2 3 Pyroxenic Pyroxenic anorthosite, Pyroxeni¢ anorthosite, summit of anorthosite, Elizabeth- Mt White- Giant trail, town face Keene valley 0 Lh AI RS helo 2-09 1-62 PUTTS sais cow ee we we oe a re cree Boe 1.00 SLO Oye: AACR ane MT ac as ele ce ses See aes I-00 RES yet a tee cues SINT hs Sh. Sv ee ee ede 4-39 on OVige te dnc S23]. ns. oe Sloe ee coe 100-14 100.54 100-990 eemercelored minerals................ 5. 83-14 81.89 85-52 MePEMGOIOned), tineralS..........sce tee ene 17-00 18.65 14.48 No. 1. Pyroxenic anorthosite from the Woolen Mill, 1 mile west of Elizabethtown. Analysis by W. F. Hillebrand in the laboratories of the United States Geological Survey. No. 2. Pyroxenic anorthosite summit of Mt Whiteface. Lake Placid quadrangle. Analysis by George Steiger in the laboratories of the United States Geological Survey. No. 3. Pyroxenic anorthosite, High fall, Giant trail, Mt Marcy Seeeerangie, Analysis by C. A. Jouet. Department of Chem- istry, Columbia University. The analyses are arranged according to the decreasing percent- ages of silica. As the recalculation shows, tower silica does not necessarily imply higher percentages of the pyroxenic constituents Since no. 3, the lowest in silica, has the highest percentage of feld- spar and the lowest of the dark mineral. Its feldspar is, however, the most basic of all, being within the bytownite ranges. In the quantitative system all three fall within class II, Dosalane, order 4, Germanase, rang 4, Docalcic, Hessase, subrang 3, Persodic Hessose. Intermediate gabbros demonstrably later than the anorthosites Special interest attaches to the two members of this variety which have afforded evidence of the relative periods of intrusion. In the case first cited, the succession has been shown by included masses; in the second instance, the irruptive contact can be fol- lowed for over a hundred yards in the rocky bed of a brook, for- tunately in a very accessible locality. The two cases will be de- scribed under locality names as the Split Rock falls, and the Woolen Mill. | Split Rock falls locality. In the valley of the Boquet river and south of New Russia there is an intrusive mass which covers 5 or 6 square miles and which is distinct from the anorthosites of the 38 NEW YORK STATE MUSEUM mountains to the westward. It outcrops in typical development at Split Rock falls, where in the cascades of the-Boquet it is well Se = ee Sa Lae : IE NSENNS AN ANNA ee SSO OS NAN =e IN SN NNN a aw DUN SUNT NON Noe NO SEE AG eg = eN Powe ae se Tare S SON aD - EERE pene --_— — aS par ak ~—= Ee 3 Ge: aS iy SS SS S ee ik of WS Oe , : = U\cero SAN Co x 1 aes . SS NSN SSSA SN SY : S <\ OG CN = SSS NSS NN ees SSSESSSE SSS NN NNN NO Fig. 5 Two inclusions of anorthosite in Split Rock Falls type, at Split Rock falls © exposed. The rock is suggestive of the anorthosites in that blue iabradorite is the chief feldspar present, but the dark silicates are ‘more abundant and when crushed and sheared the rock yields a decidedly foliated gneiss. It then becomes a hard dense rock, ex- tremely tough. Nevertheless, large phenocrysts of labradorite are ELIZABETHTOWN AND PORT HENRY QUADRANGLES 39 not uncommon and the gneiss often exhibits the “ augen”’ produced from them. Fig. 6 Inclusions of anorthosite in gabbzo of the Split Rock Falls type. Ledges on . Slide brook This intrusive is known to be later than the anorthosites because in the bare ledges along the cascades at Split Rock falls, inclusions of anorthosite are found in it. Each is surrounded by a garnet trim which appears to represent magmatic or corrosion phenomena. Woolen Mill locality. On the south side of the Branch a mile to the west of Elizabethtown and near the mill there is a very interesting rock which exhibits an irruptive contact with the anor- thosite and extends both westward and southward. It is dark, gneissoid and of moderate coarseness of grain. It resembles a rather basic member of the syenite series but has occasional blue labradorite phenocrysts which ally it with the anorthosites. Under the microscope and in slides from specimens without the labra- dorite phenocrysts, the minerals are, rather deep green pyroxene, sometimes showing faint pleochroism to yellow, plagioclase, ortho- 40 ' NEW YORK STATE MUSEUM clase, quartz, garnet, magnetite and pyrrhotite as the chief com- ponents. Apatite of course appears in occasional crystals, and biotite is moderately frequent at times and again rare. The same is true of hornblende. The individuals, except for the rare pheno- crysts rarely reach 1 millimeter in diameter, ranging from .25 to .5 millimeter. They are irregular in shape so that the rock is finely granitoid in texture. It is rather dark gray in color and is strongly contrasted with the anorthosite against which it lies. The rock has undoubtedly been granulated to an appreciable degree by pressure and crushing. The edges of the components frequently show: strains under crossed nicols. Two analyses have been prepared of the gabbro, one from a locality just below the dam at the mill, no. 2; and the other, no. 3, of a more acidic phase farther up stream. No. 2 is by Dr Waal: Hillebrand and was made in the laboratories of the United States Geological Survey; no. 3 is by Dr C. A. Jouet in the laboratories of Columbia University. No. 1 is the anorthosite and is repeated from p. 36. I 2 3 SiO ek aerk 2 ee ee 56-94 47.16 50-54 v5) Paes er cna eran Do MR arte wenn A So Se 20.82 14-45 21.28 Pies @gta conc Sotelo etetete ie tous tee i epi wove eee .83 Ton 3-43 1 © te ean Para ee eee ah ae PR aae eS ha 3 ca Loe a 2702 ieon 8-73 WW Ife] arnt ibis (eB dee egBraale, ajo cee 2 gto Ba Sala a.af 2 B26 Sey 2.08 CAO LUE oe ree ape leon ety tee ea ee cieee Q.4I 8.13 8.72 PNET © eee Oe oer eA Ae Se IB de cee, See Ours Be AS 3.09 2-95 Kei Oe oh sn 5 Pui ie ne eee 1-58 L-20 163 | GLA © es eee ee GR ENE er erase eM, nie cen phorn Gisec.o: 2 .59 48 35 AO Sas ie i ae hes Tate Se Ee ee .21 .12 06 (Sl Oy nin aa MEN coy te Pa ee come eR Ai ia min Raat “Ral -45 25 preseme FRE OR Gees ap eas ieayieiany ae LR RN A rien OB CMA ASN, comic -44 3-37 ieheneusiamets ES Sika fe Late kn MO Te bebe oe SA tamlty S eOP Tt Bees 507, 7) © i/o eae WOO. See ah eh es eno ie Wa 24 40 4 2 EH) Reimar enc erane SUE «Scot NT attr ser Nhe Chaucer ea a0) eMC SO oS oc os 3 oS ch act NNN see ge celta a ei RRR IEA Sgt Gt = ae Stal 64 IN OIG OO ede he Guest ee eae os eae Ieee as Oy aura noe O28 Pen ii 2 3 (GRE mam make te cpate ie SRS SNS NAN AANA mK xXx AN SARA NS SSS SN FAS SSSR SSS «x KANNAN ZKN RGN SSSA SAE SENG \XB SN BIR *K KWAN BR HSN : NN NS] Km KKK SVS x XK XK PAANS BABS S\SY NN SAO QA KARR ROORANN BB SN WAS KKK KK KM HK x SN UNANAN KKKKKXKKK KKK YK K XY ¥x kK NSN SNA KK KK KKH KK HH RM WK SNARE A Px KEM K CK KX HH RK F ERASASSS SSS SARIS AS “Ny HICK HK CK x Boga SN SSA SASS AS SSNS ~+-KK KRY He SNISSINGN NININ NES AE OSES ENESIES pO KX SNANS SSA NASSSNANSS SUNS aK SSNS ‘ SASSER : : EAH HX KK HK KX KX KEK XK SSRN SED EONS - 2 % So OED OOO OECD ESS ODS OSES ODES 6 6.04.0 OF Ue SAAN AN NINN NZI NINN BKK WOK IKK HK WH IK KK IIE KI OK KK HI IK OK EK IKK IS OE \\ SESS : HK HK OK WO OH HK 3g EK 9 DO EO IOK KICK KKK K KKK OK Se VAS ANNAN THK MK KK MK HK KH KM HK Kd ‘ SS KMAKK HK KKK KI NINES SAN WH HR CHM IO 3K oe KIO KC NNSANIS SSS SIS \ MAK KK KC x KX OK € -9 SINAN Ss See eck £ KKXXKXK x A c : SES ¢ 0 \ SNS oo \N\ RAN eae ent WRANS VY AV eee ptereh SAAN << oet cbc ae SS SNS © NESSES ove SONA NAN Qe NSASKSCO SS KKK IKK SSNS yuh e SASS SS SS SSS SK ROO py BARO ANS SS e N AA NASSS SOS 4 AX 8 LP KKK SSN NN LN SAN ANS KK g LPIA CK HK CSS SS SSS SSS ge) HK CHOC MK IL SAN SAAS A AASSS Kx x Kx Ky xxx SASVOs KK Goeh K XW SS Ss KuKK SOK KH «IK LARK KX Xk KOR 4 XHNX wR IKK KK > > KK YK KC Px Km WK KKK rT KS OK oO FROG OOK jw HUH WK rS) HK KC rs) ) Gg Anorthosite The ‘‘ Branch’’ 1 mile west of Elizabethtown Fig. 7 Map showing irruptive contacts of the Woolen Mill type of gabbro and anorthosite. Both are cut by a basaltic dike. ELIZABETHTOWN AND PORT HENRY QUADRANGLES . 43 former which is more abundant. There may be a little H,O in the biotite, but it has all been assigned to kaolin. The division of the CaO among anorthite, pyroxene, garnet and possible hornblende is purely an estimate. In the recasting about two thirds the mole- cules were assigned to the anorthite, while the remainder were allotted to garnet and pyroxene (including hornblende). The FeO and MgO had to be divided between biotite (a relatively small por- tion) and pyroxene (hornblende). Some FeO was also used for garnet. There is more than enough Al,O, for the feldspar, biotite and garnet, so that a small residue was placed in the pyroxene as is doubtess justifiable. All the Fe,O,; was used for magnetite, as this assumption did not yield any more than is obviously present in the slides. The composition of the garnet was necessarily assumed to involve both the grossularite and the almandite molecules. ‘There is probably a little TiO, in the rock but if so it is presumably in the magnetite for no titanite worth mention was observed. After all these assumptions, suggested or checked by estimates of the relative abundance of the minerals as seen under the microscope, the above result was reached. It is difficult to believe that a molten.magma of only 50.54 per cent silica would crystallize directly from fusion so as to yield this excess of silica forming 3.60 of quartz. If we recast without using the garnet molecule and with the allotment as usual of all the alumina remaining above the orthoclase, albite and kaolin, to the anorthite, only a tenth as much or about .30 remain uncombined. The natural inference follows that the garnet has resulted from metamorphic reactions between the pyroxene and anorthite, in which the lime and alumina of the latter were utilized and the silica left free. The Woolen Mill locality is not the only one for this variety of rock, or at least for one that to the eye appears to be the same. Blueberry mountain along the southern border shows the same general aspect with occasional large blue crystals of labradorite. New Pond locality of a peculiar gabbro. Along the road lead- ing into New pond and an eighth of a mile before it terminated at the pond itself, a ledge of a very peculiar eruptive was found, which differs from all others mentioned. It consists of sharply. angular crystals of plagioclase, rectangular in cross section, im- bedded in a dark green matrix of what proves under the microscope to be granules of augite. This rock has been seen in boulders within a mile or so of the locality mentioned and may be more widely distributed. It has also been seen in the Mt Marcy quad- rangle along the highway about a half mile south of Beede’s. The 44 NEW YORK STATE MUSEUM affinities of the rock are rather with the anorthosites than with ie basic gabbros. The relations of this rock to the other eruptives and the sedimen- taries have been nowhere shown as the exposures were so limited that no conclusion could be drawn. The rock is one admirably adapted to give pronounced hornblendic gneiss under shearing and stretching and it may have been the original of some of the puzzling gneisses occasionally seen in the region. Under metamorphism the augite would pass into hornblende and the relations of it to the feldspar are exactly those which would yield interleaved lenses when crushed and drawn out. Syenite series The syenitic series has been one of comparatively late recognition in Adirondack geology. The rocks were first identified as eruptives on the western side of the Archean area by C. H. Smyth. Soon thereafter the significant exposures found by H. P. Cushing in the railway cut near Loon Lake station on the northern side demon- strated their intrusive relations with the Grenville.” The writer has also noted briefly the occurrence of green gneisses in Ticonderoga which were suspected of being eruptive,*? but it was only after an instructive trip with Professor Cushing to the Loon Lake occurrence that the identity of these rocks was demon- strated. At times they look much like anorthosites especially in their crushed and gneissoid phases, and again they have been classed with the supposed ancient gneisses. The series embraces variations from the typical composition of syenite but the minerals with minor additions are the same and there are intermediate phases. As components of the Adirondack area the syenites do not yield in importance, even to the anorthosites, and their recognition has served to remove a vast amount oe ue puzzling rocks eu the noncommittal designation “ gneiss.” In typical and least altered form the syenite is a dark green massive rock, of moderate coarseness of grain. Its components 1Smyth, C. H. jr. Crystalline Limestones and Associated Rocks of the Northwestern Adirondack Region. Geol. Soc. Am. Bul. 6. 1895. p. 271- 83. Report on the Crystalline Rocks of the Western Adirondack Region. N. Y. State Geol. 17th An. Rep’t, p. 472. 2 Augite-syenite Gneiss near Loon Lake, N. Y. Geol. Soc. Am. Bul. Io. 1899. p. 177-92. Geology of the Northern Adirondack Region. N. Y. State, Mus. Bul- 05.) 1905. “p. 312— Bul O07 a pes ke: 3 Preliminary Report on the Geology of Essex County. N. Y. State Geol. An. Rep’t for 1893. 1804. p. 452. ELIZABETHTOWN AND PORT HENRY QUADRANGLES AS never reach the great sizes of the labradorites in the coarse anortho- sites, but range not far from the dimensions of those of the ordi- nary granites. The green feldspar is the chief component but with it are dark silicates sometimes in relatively large amount. Quartz is not lacking entirely but can not often be seen by the unaided eye. The analyses which have been prepared especially in con- nection with Professor Cushing’s work show percentages in silica which usually range between 60 and 65 or under those of typical granite but there are close relatives both above and below these values. The potash and soda are generally present in nearly equal amounts. ; The following analyses have been selected to illustrate the run of composition. None are based on samples taken in the area covered by this bulletin, but they represent all sides of the Adirondack region, and undoubtedly could be duplicated in the former. Later analyses of a series from Mineville will be given, which depart in both directions from the compositions here cited. The Ticonderoga case, no. 5, is the nearest to the Elizabethtown and Port Henry quadrangles. The sample was taken near the railway crossing of the Lake George outlet and is about 15 miles from Port Henry. As soon aS one examines these analyses, they are seen to be obviously closely akin. The low magnesia and the nearly balanced alkalies are striking. ANALYSES OF SYENITES. I 2 3 4 5 6 7 “0, See Ose Oman O07 2 04.47 8 08045) aLO2n41e) 61.01 ©".50-70 PEO a jsa.c ss. MUO On lst ehOws to 1s LOtsG. alo. 75, 815-26. “10.52 [a0 ae 1234 Te23 0h. wa I-09 2-49) P16 0. a 22 2.19 Fi OG, 2-69 4-91 10.75 | 5.65 MieOr 8... 26 78 eit 35 Or -78 -78 20) ocean 2.20 27.20 2 LO 3.06 Bee M7 4-05 3.36 I Quartz-augite syenite. Altamont, Franklin co. Analyzed by E. W momey; tor H. P.Cushing. N. Y. State Mus. Bul. 115. 1907. p. 514. 2 Augite-syenite. Little Falls, Herkimer co. Jdem. 3 Syenite, gneissoid. Whitehall, N. Y. Analysis by W. F. Hillebrand 4 Augite-syenite. Loon Lake, Franklin co. Analyzed by E. W. Morley for H. P. Cushing, who considers the occurrence as typical. Geol. Soc. Miia iG. O00. p. 177. Revised in N. Y. State Mus. Bul. 115. 1907. p. 514. | 5 Augite-syenite. Ticonderoga, Essex co. Analysis by M. K. Adams. 6 Augite-syenite. Altamont, Franklin co. Analyzed by E. W. Morley for H. P. Cushing, as under no. I. 7 Augite-syenite. Line of townships 22 and 23. ‘Franklin co. Analyzed by E. W. Morley for H. P. Cushing, as under no. 1. { 46» NEW YORK STATE MUSEUM I 2 3 4 5 6 7 NazO®.2.- 2-4. 2.50 4-36 2 ei 5-06 3-09 3-68 i ar Ke Omecisree See 5-90 5-66 2268 ia | 4.25 3-90 4-14 Hist ee iene sees ome Whew bee wee) ee a FASS on he cet eee eae eae TO. Se essa sake ue a eae Le JEU te ree tao ee, 4O ELid5 avin atc 3 30 AI 49 52 "FiQs oe i nds ce Dekel ee ene ea eereees Cae OF) ores 3 ota sheds ee a PIO sa ateser ae Oy Fister Bo Oe dict sles st ye WitiG)e eee tee ae 1K) BO Oa ues a6. tiene Rees 08 09 JBL Ne LR Beonsaones OSie liars Sasser ieee ik ee eresirorio ry sors RNS rere Meee SAO aIG ON ve ry yuh ORL airy TB a ath a Mawr tiene. «: oth th eis, canes tea ae ra CLO ents Merit ene wt oa raaee ds oe 88 OP eel. aces Oe Glen e 100.22 100-18 99-49 99-73 100.09 100.10 100-23 I Quartz-augite syenite. Altamont, Franklin co. Analyzed by E. W. Morley for H. P. Cushing. N.Y. State Wins: Bull-115.> 10072. ps5 2 Augite-syenite. Little Falls, Herkimer co. [dem. 3 Syenite, gneissoid. Whitehall, N. Y. Analysis by W. F. Hillebrand. 4 Augite-syenite. Loon Lake, Franklin co. . Analyzed by E. W. Morley for H. P. Cushing, who considers the occurrence as typical. Geol. Soc. Am. Bul, 10. 1900. p. 177. Revised in N.Y. State Miss, Bull scrsseneay Pp. 514 5 Augite-syenite. Ticonderoga, Essex co. Analysis by M. K. Adams. 6 Augite-syenite. Altamont, Fronklin co. Analyzed by E. W. Morley for i. P: Cushing, as under nol a, 7 Augite-syenite. Line of townships 22 and 23. Franklin co. Analyzed by E. W. Morley for H. P. Cushing, as under no. 1. In the quantitative system, nos. 1 and 2 fall under class I Persa- lane; order 4 Brittannare; rang 2 Toscanase; subrang 3 Toscanose. Nos. 3 and 5 belong in class I] Dosalane; order 4 Austrare; rang 2 Dacase; subrang 3 Adamellose. No. 4 is in class I Persalane; order 5 Canadare; rang 2 Pulas- kase; subrang 3 Pulaskose. No. 7 is in the same except the subrang 4 Laurvikose. No. 6 is in Class II Dosalane; order 4 Austrare; rang 3 Ton- alase; subrang 3 Harzose. Under the microscope the chief feldspar is at once seen to be microperthitic orthoclase; that is, the orthoclase of the ordinary syenites is filled with flattened, parallel blades or spindles of albite. This’ microperthite is very characteristic and with the beautiful emerald-green pyroxene affords one of the distinguishing features of this group of rocks. Plagioclase is not entirely lacking, and es- pecially in the specimens from Mineville is at times quite prom- inent. Quartz is variable. As will be shown later there are phases, apparently differentiation products of the syenite magma, in which -ELIZABETHTOWN AND PORT HENRY QUADRANGLES Ay, it is very abundant, and the rock becomes a granite, or of granitic composition. In these the quartz is very abundant. Again in the basic extremes, it fails, and in the true syenite phases, the most characteristic of the series, it is rare or absent. The most prominent of the dark minerals is a beautiful and striking emerald-green pyroxene. It has the high extinction angles of augite, and sometimes a faint pleochroism to yellow. Experience gained in recasting analyses leads to the conclusion that the jadeite molecule, Na,O, Al,O,, 4510., is present in its composition, and may be largely responsible for the beautiful green color, so sugges- tive of aegirite. The pyroxene often changes to chlorite and when present in the bodies of magnetite associated with the syenites, it yields red oxid of iron and stains the ore red by filtering into the cracks in the neighboring minerals. It has the same effect on the syenitic rocks, especially those associated with the ore. Under the miscroscope the reddish tinge can be traced back to the chloritized pyroxene. Hypersthene is occasional in the syenites, but scarcely so abun- dant as to require extended description. Hornblende, however, is very common. It is a deep brown variety and in the basic types may be more abundant than pyroxene. Biotite is known but is subordinate. The basic phases have it more abundantly than the acidic. It is deep brown in color, but not otherwise remarkable. Among the accessories titanite is sometimes extremely abundant. To the unassisted eye it might be taken for garnet, and in the acidic phases, associated with the magnetites, it makes this impression, but the microscope, of course, reveals its identity. Apatite is at times noticeably abundant but presents no peculiarities worthy of special remark. Zircon favors the acidic extremes. Magnetite is in all varieties, even the most acidic, where, unless sharply observed, it might be mistaken for a dark silicate. Pyrrhotite is rarely to be detected. | hue! In earlier experience it was believed that garnet was practically limited to the anorthosites and basic gabbros, but as the tendency of the syenites to develop basic phases has been appreciated and the dark hornblendic gneisses have seemed to be, in part at least, referable to them, garnet has been recognized as one-of their minerals. While, the reaction rims, which will be more fully described under the basic gabbros, are far more abundant in these latter rocks, yet some cases have been observed in which they were also apparent in the syenitic gneisses. Some dark, hornblendic gneisses have, in the later field work, shown such relationship as to } 1 48 NEW YORK STATE MUSEUM be referable to the basic syenites and not necessarily to the gabbros, as formerly believed. Field. associations and preponderance of orthoclase as seen under the microscope must hereafter decide. On weathering, the syenitic rocks are particularly prone to de- velop a rusty exterior although just why the contained iron is in a condition so sensitive to alteration, is not apparent. When one seeks for a fresh hand specimen from fallen blocks, it is often necessary to pound off several inches or the better part of a foot before the fresh green rock appears at the core. Where polished off smooth and hard by glaciation, the rock may also develop a very white coat or skin which, however, is easily chipped off so as to expose the fresh green beneath. The relative proportions of the several minerals vary widely over extended areas. Toward the acidic extreme, quartz may become increasingly abundant, fully enough to carry the rocks over into the granites. Such varieties appear on Barton hill near Mineville and in association with the ores of the great mines. Yet the microperthitic character of the feldspar is pronounced and the same augite and hornblende are in evidence which we find in the typical specimens, so that one can not well avoid the conclusion that there is a fundamental relationship. | Very instructive evidence has been afforded by the numerous diamond drill cores which have been obtained in. the explorations for magnetite at Mineville. The writer has examined most care- fully thousands of feet of these, and finds on the whole the average syenite most frequently present, but with no evidence of being a separate intrusive mass. The most acidic variety will quite sharply replace it; and in the same way a very basic variety may come in and constitute the section for 50 or 100 feet or more.” Vet while the transition is sharp there is no evidence of separate intrusive masses nor is one justified in inferring more than a differentiation of an eruptive mass into layers or portions of contrasted com- position. As will be later shown in speaking specially of the ores, the great body of magnetite lies immediately beneath the most acidic phase. The ore contains appreciable amounts of the emerald- green pyroxene and is simply an extremely basic concentration of one of the normal minerals, the magnetite, accompanied by two others, the pyroxene and apatite. Beneath the ore, usually if not always, is found a basic phase of the syenite. All these relationships will be more fully discussed from the standpoint of the ore on subsequent pages, the object being at the moment to emphasize the variability of the rock mass. ELIZABETHTOWN AND PORT HENRY QUADRANGLES 49 In the Ausable quadrangle very rusty basic dikes of the syenite series have been found, intrusive even in older and larger masses of the same series of rocks. The basic syenitic types develop under metamorphism a crumbling variety of gneiss, which on exposures that have been quite thoroughly weathered may be rubbed to coarse sand between the fingers. Black grains of silicates and ores then separate from rusty green feldspar. Within the area here described all varieties of syenites show the effects of crushing and the production of gneissoid foliation to a marked degree and no locality can be cited free from it. Along fault planes, where dynamic effects are pronounced, much secondary quartz has sometimes been infiltrated and on weathering the rock becomes a pronounced red, looking like a coarse, red granite. This so called syenite series has an exact parallel in Norway, where in association with anorthosites, practically indistinguishable from the Adirondack occurrences, C. F. Kolderup has established the existence of others consisting of microperthite and augite. The latter Kolderup calls by the new name mangerite, based on a Nor- wegian locality, Manger. This duplication on opposite sides of the Atlantic is an extremely interesting coincidence.? The following analyses have been prepared of the syenites within the area covered by the bulletin, three of the samples having been taken from drill cores at Mineville. They represent the several varieties as well as selections would admit. With them is also placed one of a marked granitic phase, no. 1, which, however, care- ful study of relationships fails to prove a separate intrusive mass. I 2 3 4. oo 2 a=) dls 2 Ss eee 68 .87 73.84 52-01 45-81 oe Ea 10.76 14-11 16.93 20.32 5. lig 3 Sega 3-52 «22 -14 -53 tL ee a RSS los Kal2 10.25 8.45 RP Se ee eee ae 2227, 83 2.50 6.45 MUM ek ee 2.50 44 6.14 7.7 MMe crc tece Fie cv bie a dies ee NAS 6.36 4.65 A. 53 I Granitic extreme of syenite series 1 mile west of Mineville. Analyzed by Charles Fulton. 2 Granitic extreme of syenite series; hanging wall of magnetite. Mine- ville. Analyzed by M. K. Adams. 3 Average syenite of rocks containing the Mineville magnetite. M. K. Adams. 4 Basic syenite of rocks containing the Mineville magnetite. M. K. Adams. ~ 1Kolderup, C. F. Die Labradorfelsen des westlichen Norwegens. Bergen’s Museum’s Aarbog. 1903. p. 102. 50 NEW YORK STATE MUSEUM I 2 KO etek cee ote en enone 7.88 2-38 FISOA Ec Be 5 ee ec ere oe ee eae AO ET OE ec Oates ve cuusce mundane aren snone II COs ok BAe fe as be OR ee ee 16 Paha. Save Sieger tee rae eke ere nee ea 14 46 Zit Ore ae ie Le cee ae ete ole ee ae eee nee rele) 12 © Pare ey ees we PgR ET ASD tel ck eR Heo od: -06 Serer ee aceon hs oes Hic cat eae haa. Lip ce eas His “07 10 Bik @ eaerenaineinae Serta ne Une n a ork oh iaoe ny A aty'S "AS “O38 Bai Ore Aa ete eee) Sasceeratt nd ce Mee pesemrereteer Ese none Cts Og vu. sere eistecalgs aire Sheen hocks ea BER nee none vk omen 100.74 CES re ae Se ares ae ee potere ten eee ae -03 TE Otal 22 ve wthioe act heen aon 99.74 100.71 I Qin riy Anon Meta temo eros att on a vgléoe ane e S 21-540 Ortho clases eas otis teetabe ee ole acon tier ee eI ee cars 36-696 AdBite Go PRA eco te ere eis 20.960 Kaolin 20. yale es bad ice ae ke Sere oe eee Re ae Caleta. ecg Sissies ee Ca eae ee aera "Vettalinnt © iti Ae rd al ee ee fede te eee eat .198 ZAVCOD. ice ee ae Ok Re Oe ee CaOrSiOs vee lt near orca eae men eee 5-336 Mie @©: Si@siess wee some ecg care oi oe ennen 3.800 Wi ktes @ aad OPRSI © Anne AS Aces bad gatetee cn) coe ke Be@eSi@)s Birth cae Se tantere cnet etre oe ener : 1.848 MipnOe SiO secession a BUKEO sesOg Soi Oyun, seitectanteteneranee nice 6-732 ANd Olecul Ona Ne, Pore oor ct sormelc aca wed et ols Cone oe 1.260 MWkateran et iel ae ni tes ee rece ee easton ott ae ear .928 NiG OPAL Or wih: meister anew RSPR, See mUe Me ON? Ba cAI din A Pyrrhotite Pay eas SRNR HAY igi NEEL urea ae she Se Pit a INIA ed POO ao oe ode. woe. no Say we 1 St © aed a Set tons ee eran eR Ma A ore mE eonmene 2 CO5 CR CESS 8 Feito cee ae atts pa net ae gga get ene eed Ppa Sabb ees 8 ie orale ieee arte oes fs Baa WY) Bok © Mere trae ee etariseae mo rere irene Oka ye Tal inn eet ue a SNe otal sera rig ae nam clea ree eae eae ee 99.298 Cricpecimo. eetacy. 1 eeeere 6 8 o eoeeceeceese ee cee e ee eoecoe ee ve eee eres eae 100.410 1 Granitic extreme of syenite series 1 mile west of Mineville. by Charles Fulton. ee ee 8 ee eceeeceee ee ee ee oe es ee @ eee ere e ee ee eso ee ee @ © ere oes ee 100.031 Analyzed 2 Granitic extreme of syenite series; hanging wall of magnetite. Mine- ville. Analyzed by M. K. Adams. 3 Average syenite of rocks containing the Mineville magnetite. Adams. 4 Basic syenite of rocks containing the Mineville magnetite. M. K. M. K. Adams. ELIZABETHTOWN AND PORT HENRY QUADRANGLES 51 Endeavors to recast these analyses according to the mineralogy exhibited by the thin sections have not been very satisfactory. No. 1 has involved several assumptions. The soda was first all assigned to albite. The remaining alumina was used for orthoclase, there being none for anorthite. The residue of potash, with the necessary ferric iron, was used for biotite, affording a variety ab- normally high in the alkali but making very little difference in the gross result. Everything else was assigned to hornblende, except Semetne little magnetite and titanite. The slides reveal quartz, microperthite, biotite, hornblende, magnetite and zircon. No. 2 presents no difficulties. The great preponderance of the light colored minerals is striking, since about 95 per cent consist of these. The remainder is chiefly augite although this mineral is a very obscure component to the eye. The richness in the albite molecule is striking. While this mineral is chiefly observed in microperthite, it can not obviously be altogether in this form, since Meeeper cent orthoclase could hardly contain 53 per cent albite. While this rock is believed to be an acidic differentiation product from the syenitic magma, it is only fair to state that in one respect the analysis is similar to the usual run of slates and argillaceous sandstones, in that with high silica the magnesia exceeds the lime. The opposite relation usually holds for the eruptive rocks. Yet the amounts are small and other considerations lead to the interpre- tation as an igneous variety. The presence of zircon in the acid member and its failure in the basic is an interesting corroboration of our ordinary conceptions of the home of this mineral. When the recasting of nos. 2, 3 and 4 are undertaken, difficulties arise in providing so much soda with sufficient silica to satisfy the albite molecule, at its ratio of one soda to six silica and yet have sufficient silica left to form unisilicates which take up the other bases. One can not but infer that the emerald-green pyroxene itself carries soda, but it can not be in the form of the acmite molecule, Na,O.Fe,O.4Si0, since we have so little Fe,O;, while magnetite is a certain component of the rock. The alumina is also in excess, and can only be provided for by the spinel molecule. Yet no spinel has been detected in the slides. Any form of the olivine molecule, and any corundum which we would use according to the methods of the “ Quantitative System of Classification of Igneous Rocks” are also not to be observed in the slides. Nephelite can also not be detected in the slides although with basic rocks such as these, the rather high percentage of soda would seem to call for it. 52 NEW YORK STATE MUSEUM The chemical analyses also throw some light on the question of their igneous or sedimentary nature. It will be observed that all the rocks are rich in soda, even the most basic. Were they re- crystallized sediments, they must have been derived from shales, or in the most acidic cases, shaly sandstones, since no other sedi- ments will give anything approximating these compositions. Yet in the process of disintegration of feldspathic rocks and deposition of the debris as sediments, the alkalies diminish greatly and of the two, potash is customarily the survivor. Sediments of a com- position such as these analyses afford, would be extraordinary, whereas eruptive rocks not infrequently furnish parallels. Granite. This rock as an acidic extreme of the syenite series has already been referred to. The field relationships of the speci- men analyzed are best explained by this assumption. In the south- eastern corner of the Elizabethtown quadrangle, there is, however, as already set forth a quite extended area in which granitic rocks are prominent. It has been mapped as a separate mass, although the evidence of its individual intrusive character is not clear. The subject is fully discussed under the topic of granites and related types. They have a widespread reddish color and yield percentages in quartz such as are possessed by the granites. : In one of the two localities which have been studied with the microscope the rock consisted of quartz and microperthite in great preponderance. There were a few shreds of biotite and hornblende, and rarely a grain of magnetite and a-zircon. The rock was greatly crushed and strained. This is the specimen which furnished the analysis given as no. I under the syenites above. A second, a reddish rock from the southeastern corner of the Elizabethtown sheet in the area mapped as granite, contained greatly predominating quartz and finely twinned plagioclase. It has already been mentioned under granites on a preceding page. Orthoclase could not be identified. A few decomposition products, believed to have once been bisillicates, and a few tiny zircons made up the slide. The minerals showed abundant evidence of strains -and crushing. Basic gabbros This type of rock constitutes a large number of intrusions well distributed along the border of the anorthosites and the other rocks and sometimes in the anorthosites themselves. They are wide- spread throughout the eastern Adirondacks and, although far less large in amount than the anorthosites and syenites, are yet a char- acteristic feature of the local geology. They appear chiefly as ELIZABETHTOWN AND PORT HENRY QUADRANGLES 53 irregular masses of moderate size, and are sometimes demonstrably in dikes. More often they seem to be irregular, eroded sheets, knobs, or perhaps laccoliths. The abundant vegetation, the wide- spread faulting, the extended erosion and the metamorphism, have all served to mask the details. OTIC LAX CFF SOL PLECLSLAR KY SOS SL EU ARS 7 LAOS, RIL LR MIE TL LTT TL x VIL SASAXX XT TSS 77 SR IX TLS STS OD) LALA EIIRX MSS LL LT GPL LIME L LAS LT, YAUSEFANKXSS 1 IT TTL SAIS LIAXKIA SS SSS LT ln PAI TEIDOOL SS AS TTL PILSIS MNS ST SL fT SSP LIXAY ALAS SASS. LAL A'S XxXY 1G i CATS IOC ONL dA) Det. 0 iy My A = ¥/ LS Laff | OLY BA NE el oe ee t— 0". 6 Ai ° 6.5 .ehue. of De ODA EM LEIS GY fo eS BY St WSS*AS TSS 7 Ie Lae eae SEL AA GLE ASE: Dt DLT TS, VEG be hey a VEG kth eh Gabbro Gress Fig. 8 Gabbro dike intruded in anorthosite and faulted. The gneiss is either an inclusion or a dike older than the gabbro, and greatly sheared. The locality is in Lewis in the northeast corner of Elizabethtown quadrangle. The rocks are greenish black in color and rough upon weathered surfaces. The pitting from the decay and disappearance of the feldspar has left the augite and ever present magnetite projecting in little lumps. Where the gabbros appear in the beds of streams and beneath cascades, the rock is a rich green and affords most beautiful and instructive exhibitions of rock texture. It is com- paratively rare that the gabbros are free from the effects of crush- ing and shearing. When, however, such specimens are found they present a coarse diabasic texture. The plagioclase crystals are tabu- lar and on the fractured surfaces exhibit thin rectangular cross sections within whose network the dark silicates and the iron ores 54 NEW YORK STATE MUSEUM are packed away. The ever present effects of pressure have almost always granulated the components and have turned feldspars, bisili- cates and ores into lenticular interwoven masses. More complete crushing, often accompanied by apparent flowage, has given swirl- ing, gneissoid foliation and in the extreme has developed a decided hornblendic gneis.. This curious and interesting variation of tex- ture can be seen.in the brook bottoms which enter the Boquet from the steep mountains on the west, and above Elizabethtown. The brook which comes in about 2 miles south of the village and along the contact of the gabbro and syenite and with a trap dike across its exit from the cliffs, gives very interesting exposures, and the same is true of Roaring brook a mile to a mile and a half from its mouth. ‘The stringing out of the minerals may be in part a phenom- enon of igneous flowage, but certain it is, that the textures vary greatly within short distances and the rock, whether molten or — whether viscous from pressure, has not behaved as a perfectly hydrostatic body. Buttresses or masses unaffected by the flowage have remained in the midst of the generally plastic material. The component minerals of the gabbro are chiefly plagioclase, augite, hypersthene, brown hornblende and titaniferous magnetite. The less common ones are olivine and biotite. A widespread mem- ber not truly original with the rock is garnet, which appears in the reaction rims in a very interesting and at times remarkable manner. The plagioclase is a basic variety, labradorite or one even lower in silica. It is so charged with finely divided dusty inclusions that it remains practically opaque in its central portions even in very thin slides. The inclusions appear to be pyroxenic dust and minute green spinels, but they are so exceedingly small, and their optical properties are so disguised by the containing feldspar, that their sharp identity can not well be made out. Around the edges the feldspars become clearer, and next the reaction rims of garnet they are limpid and transparent and apparently are untwinned albite. The lime component seems to have been contributed to the garnet. The augite is, in the thin sections, light green in color and ap- pears to be of the ordinary variety, often seen in the gabbros. The hypersthene is widespread and frequently in sufficient amount to make the rock a norite. It is in no way remarkable. The horn- blende is of a deep brown variety, and increases greatly in amount where metamorphism is more pronounced. Olivine is not specially abundant. So far as studied, many exposures may entirely fail to show it. It is pale green in color and customarily quite fresh. The titaniferous magnetite is richly distributed through the rock. It can be readily detected with the eye, and under the microscope wey oe, ae Se be “? AI. * “Raighe 444 o® ELIZABETHTOWN AND PORT HENRY QUADRANGLES 55 forms basic centers around which are grouped the bisilicates in especial richness. In several places the titaniferous magnetite has become sufficiently concentrated to attract attention as an iron ore. The ore yields about 40 per cent iron more or less, and can be best discussed under the topic iron ores. It is simply a portion of the gabbro mass with an unusual amount of the titaniferous magnetite. The feldspar fails but all the other components are distributed > through the ore and appear in the thin section. The reaction rims of garnet are very widespread in the gabbros, so much so that it is unusual to find the rock unprovided with them. They follow along the border lines between the feldspar and the more basic minerals, preventing the contact of the two, and giving a pinkish cast to the rock which is quite characteristic. The garnets at times manifest a curious tendency to develop projections like fingers out into the feldspar and seem to have formed from one twin lamella and not from those on either side. A number of analyses of the gabbros were prepared several years ago in the laboratory of the United States Geological Survey, in connection with a paper by the writer, upon the “ Titaniferous Meso tie Adirondacks.” They are reproduced here in order to give an idea of the chemical composition of the rock and to fur- nish a basis for recasting into the approximate percentages of component minerals. With these quoted analyses are one or two others from exposures not connected with ore bodies and only hitherto published in Bulletin 168, United States Geological Survey, page 37 under the work of the chemical and physical laboratories. : at 2 3 4 5 tw Pe ot 47.88 47.16 46.74 44.97 Bae eT PO % a20-. 18.90 14.45 16.63 I5.40 12.46 Fe,O, Te39 1.61 2.17 2.29 4.63 Be... I0.45 eee St I0.60 12.39 I2.9¢ EEO sch... 7.10 5.24 6.11 10.89 5-34 ae 8.36 8.13 8.66 7.50 - 10.20 a5 aeons 2.75 3.09 3 85 3.02 2.47 0 esas 's St es . 86 -56 ROS | == 482 -43 a4 e073 65 48 — .18 .12 aie .I0 .I2 ae Beeps, «2 .12 Bie Kens 23 | ae I.20 3.37 2.54 1.18 5.26 ae .20 “Ey LBS Sai .28 | ae .07 .14 Sree .06 .26 _ aa 26 -24 .206 .22 .17 NiO.CoO... .02 .02 .03 .02 shel a a a Tr ar aC ew MIE 6 Wewere nolo tala I00.02 99.98 O77. 99.72 Le LOO is 1 Wall rock of titaniferous magnetite. Split Rock mine, Westport. Analysis by W. F. Hillebrand. . 2 Woolen mill 1 mile west of Elizabethtown. Analysis by W. F. Hillebrand. See above Cae 3 Gneissoid gabbro, 2 miles south of Elizabethtown. Analysis by W. F. Hillebrand. 4 Massive gabbro, same exposure as No. 3. Analysis by W. F. Hillebrand. 5 Wall rock of titaniferous magnetite. Lincoln Pond. Analysis by George Steiger. roth An. Rept. 1899. pt III. p. 377-422. 50 NEW YORK STATE MUSEUM I 2 3 4 5 ne PEED, ith sags G23. ae. 3-34) 5:00 A vedednnc het ena 2310 26.20 Bit OIG) Aye hs) 20.9 Ha ae 33.604 50.70 18.07 f ae ci 13.90 f 45 87 13.34 J 38.49 16:40 | 37.36 aolineeae 3.10 BAS 5.42 4.65 3.60 Calcitetaee .20 .80 Io 50 -90 Sat eaa 2 Si 2 II 25) 3.48) 12.53 MeO.siG,. 2 sical 8oeS5 eee een r Go| 9-06 2 7ee ae nO ae 26 “40 | 58 2 26 | 2FeO.Si0.2. 8.46 8.36 10.20 T3047 Teg gue Oe Oa: Sosy 16.93 ere) 13.82 eh 19.16 16.80) 3° 47 1.20 ies agnetite.. 2.09 2.32 3.25 S25 6.73 Ilmenite... 2.13 6.23 4.62 2.16 9.73 Apatite... -34 1.34 70 3315 .67 Pyrrhotite. .18 a5 .26 .18 555, eed ae sie Ra tea ea ees Lime: era T2023 ee ORGS) UA ep Met lances el al DM 2 a ein Bi 5 WS} ee ie A EE a I 2 3 4 5 Pilacioclase:recincl eee ere eens ae Ab,An., Ab,An,., Ab ,;Ang..s Ab,An, © AbjAny.5: Light colored minerals......... 64.45 SoA On sO ee OReG 46.86 Dark colored minerals......... 35.08 43-95 43.10 52.40 53-42 ais of titaniferous magnetite. Split Rock mine, Westport. Analysis by W. F-. agen coe mill x mile west of Elizabethtown. Analysis by W. F. Hillebrand. See 3 Gneissoid gabbro, 2 miles south of Elizabethtown. Analysis by W. F. Hillebrand. 4 Massive gabbro. same exposure as no. 3. Analysis by W. F. Hillebrand. 5 Wall rock of titaniferous magnetite. Lincoln pond. Analysis by George Steiger. In the quantitative system, no. 1 is class II Dosalane; order 5 Germanare; rang 4 Docalcic, Hessase; subrang 3 Persodic, Hessose. Nos. 2, 3, 4 and 5 are all class HII Saliemane; order es (Gallanc. rang 4 Docalcic, Auvergnase; subrang 3 Auvergnose. In recasting the above analyses, nos. 1, 2 and 5 could be done in the normal way. ‘That is, aside from the accessories such as mag- netite, apatite, pyrrhotite, ilmenite and calcite about which there can be little doubt, the soda and potash were assigned to albite and orthoclase ; the combined water to kaolin, and the remaining alumina used for anorthite. There then remained sufficient silica to care for the excess of lime as the bisilicate and for the ferrous iron and magnesia partly as unisilicates, partly as bisilicates. In nos. 3 and 4 this proved impossible, because if this course is followed for anorthite there is not enough silica to satisfy the remaining bases even as unisilicates which we know are not the sole dark silicates present.. To obtain sufficient silica, the only feasible course was to reduce the anorthite, ‘and for no. 3 a plagioclase imoleeme Ab,An,., was assumed. It became possible then to reach a solution. In no. 4 similarly Ab,An, was assumed, and both the garnet and spinel molecules were called in. These assumptions have no par- ticular advantage over the ordinary calculations of the highly ingenious quantitative system, except that we confine ourselves to making assumptions of minerals known to exist in the rock. Probably every one of these rocks had some garnet, to whose substance both anorthite and bisilicates contributed. Possibly ELIZABETHTOWN AND PORT HENRY QUADRANGLES 57 some of the ferric iron was in the bisilicates and it was not entirely combined in the magnetite. The calculation of the pyroxene does not tell us how much is hypersthene and how much is in the mono- clinic variety. Probably some little alumina was in the pyroxene. Yet even with all these restrictions the final results in nos.:1, 2 and 5 are doubtless very near the truth and afford interesting general conclusions. Thus no. 1 is only 3 per cent higher in silica. than no. 5. Yet the light colored minerals are almost 20 per cent greater in the former than in the latter. The excess of alumina in no. I is mainly responsible for this result, since by this we are able to care the better for lime in anorthite. It is striking that silica should fail to satisfy the bases in nos. 3 and 4 on the lines of the ordinary silicates, despite the fact that in these rocks its percentage exceeds that of no. 5, and but slightly yields to nos. 1 and 2. Mineralogical relationships in rocks, as indeed we have learned forcibly from the quantitative system,-depend on other factors than the silica. With all their shortcomings these recast analyses are nevertheless presented with the purpose of illustrating again the connection be- tween chemical composition and mineralogical components. Unmetamorphosed basaltic dikes The last manifestation of eruptive activity and one which fol- lowed the general metamorphism, took the form of comparatively narrow basaltic dikes. They are quite widely distributed but not specially abundant in this area. They are members of an eruptive series which is widespread throughout the:eastern and northern Adirondacks. Approximately 20 individuals or groups of individ- uals have been noted in the Elizabethtown quadrangle, and 16 in the Pott Henry. These are. undoubtedly but a small fraction of those existing and either concealed or unnoted. Wherever cascades reveal exposures for relatively long distances or iron mines have opened up the rocks underground the dikes have almost invariably been discovered. The great majority strike northeast. Of 32 @ecuirate records, 19 lie between n. 35° e. and n. 70° e.; 6 are east and west and 4 nearly north and south. Only 3 are northwest. The northeast strike corresponds with the major structural breaks, and the dikes often appear in the broken and jointed rocks where exposed in the beds of brooks. The dikes are mostly narrow, from 1 to 4 feet, but one has been met at 40 feet, and at the other extreme there are some only a few inches. Where the dikes tongue out to a feather edge, they 58 NEW YORK STATE MUSEUM become a coaly black glass from the effects of chill, and always the borders are denser than the centers. 0 20 ft eee | SAAN S\N et ORR SERN N SNNNSNONS [AN NAS ANS RS SSSR SSNS LN SIR SESE SASS SSS NI SN One very interesting case has NS SS SES SSS Fig. 9 Step-faulted dike in Walker brook, North Hudson been found of one dike penetrating another and chilled by it. There were clearly two periods of intrusion in this instance and — Tra. Dik »vO Anetss AES KOCK N NANA N NOS Ne SEEN CYL KLNRA NN ALK QRINNN NYS NNNA we NNN SAAN SN NN ANN NSN SN SASAY CX NAAAN SNS SN NSN NLA SK OYA LL NANA SA Sf VX MANA RK LNA RRA AN NAN AN SABES NNANNS NEN RQ KN ANAK BRN NL SNAN cen KLAN ARN NBN NN NAN SS NAAN AN AKA AKAN NNN NNNANNNS NNN RNS KAA NAAN S MBBNS SAAN SS NS KN ARN AINN AN ALAN NMBBANNN ANAS AS NAN OD RA NRNNS ARMS NNANANSS SN NANAIAN ANNAN RARE NV NNNANINNN NNN SAR \ SAAS NIA NA NSBBRANANN AS AAAS KXAN NNANNA INNANNNANANNNSN PASANNIR NINN NSN LLUNNANN NANNS N NAS] OSD SN NAY ANC NANNANNNNAS NAN A(ASABN NN CA RXNNSAAN KASS SAN SSeS ENN ANN NAAN A NSS NANA ASA INGE NAN NN RAANSNAS NS A ANN SIS NBBAS MSS YSSQLLNS SA RANA LA JN NALANANSA ANNAN SAN NA SNS SAUNAS NOON) NANSAANN NANOS NS NNN NON AGN RENACN ALN NN ANNES ONAN SONS AGSA NS SSS NS NN\ NS NANI NAAN NX ANCNGN See \\\g TU SARS >” —& N NANNANANX NAN SSS ‘iS \ NASON NN SSS NN V VRAIN ASSN NN CN oO IS 30 N\ i \ | Fig. to Basaltic dike in an irregular and jagged crack on Slide brook. The dike strikes NM. 15° e. and dips ao°least, The wall rock is gabtro of the Solit Rock Falls type. si — >. — ELIZABETHTOWN AND PORT HENRY QUADRANGLES 5G one followed long enough aiter the other to have permitted the first to quite thoroughly cool. The specimen came from a boulder in the bed of the Branch, 2% miles west of Elizabethtown. The dikes sometimes present extremely interesting exposures. Figure 9 was sketched in the north fork of Walker brook in the extreme southwest corner of the Elizabethtown sheet. It shows some very striking little faulted blocks of a dike in anorthosite. Presumably the dike was once continuous but in being broken and separated into the little blocks it held its sharply angular form while the anorthosite which is here much crushed and granulated, molded around it. Figure 10 shows a dike in a jagged crevice. Figure 7 is a map of a small dike which appears in the bed of the Branch just above the mill, about a mile or less on the stage road from the Windsor hotel to the Keene valley. It can be followed O E SoS NSN NN N NANSANANNNS NK SSOSNS SON SAAN SHINN Re SS x 4 \ XN = l RAN NANN SAS NERS SS SA KNESSET SS Leo eS O N Cc e Fig. 11 Network of basaltic dikes in anorthosite and crossing the bed of Slide brook The dikes strike n. 45° w. in the bed of the cascading brook from one end to the other. Figure 11 illustrates an interlacing network of dikes. These dikes must have entered the wall rocks under very great pressure, and while in a state almost as fluid as water, must have penetrated every litile crevice and crack open to them. They ob- viously followed the chief structural lines of weakness, and prob- 60 NEW YORK STATE MUSEUM ably represent the last basic dregs from the great center of erup- tion which gave rise to the larger masses. In all cases noted they are massive and unmetamorphosed except from weathering, Un- doubtedly they followed the great period of metamorphism but shared in some faulting. Under the microscope the dikes are distinctly basaltic in their mineralogy. Plagioclase and augite are the chief minerals. Olivine occasionally appears, and magnetite is of course in every slide. In the thicker dikes and at the centers of those of moderate width the texture is diabasic; that is, the feldspars are long and narrow and well bounded. They form an interlacing network in whose interstices are the dark silicates. Toward the borders, however, the texture becomes porphyritic with a finer and finer ground mass until at the border the ground mass is a dense, black glass. The dike is cemented at times so tightly to the wall rock, or fused into it, that it breaks more readily elsewhere than along the contact. In several instances where cliffs are exposed along the course of a dike, fragments of the latter may be seen, still adhering tightly to the older walls, although the major part of the dike has disin- tegrated and disappeared. These relations appear at the dike shown just west of the highway and 2 miles south of Elizabethtown, and also in the one on the northwest corner of New pond. No analyses have been prepared of the dikes within this area, but a selection is here given of those which have been published from neighboring localities. They will also be found compiled pre- cisely as here given in New York State Museum Builetin 95, page 350. : Thy 2 3 4 5 SOs serge eae sais oe 43-Al 44.51 45-46 46.73 50-89 ACT (Ch boas tae eed taverns 19-42 19.99 19-94 16.66 15-39 ies Oar auc sees aie sostents meee ORG ey/Z 2250 ESO ave ee ae 160 ies 15:30 ae 5-77 MeOK 2 mG eee Se A508 8.11 2.95 S02 7.60 GAO) eke ee Q LE 8.15 S382 8.03 8.75 Nas Or tree eran ees 4-39 Spnayit 2.12 B19 Oy, 1 Diabase summit of , Mit. Marcy, Essex ‘co. . A. R, Weeds, SING yee ours Mus. 30th An. Rep’t, p. 1e2. 2 Diabase.. Upper Chateaugay lake,. Clinton co. A. S. Eakle? Ama Geol. July 1893. p. 35. : 3 Diabase. Palmer hill near, Ausable’ Forks, “Clinton IS ~A ~ sy gs x. ~. TN ._~ ‘ SES Wace . SKA OSS SS ~~ s CO wees ae oc A nee eS NS ANS ns a Fig 26 Sections 21 and 22 of Old Bed ore bodies, Mineville. See figure 19 120 NEW YORK STATE MUSEUM Fisher hill mines belonging to the Port Henry Iron Ore Co., and the Burt lot, of Witherbee, Sherman & Co. The ores are rather lean but are of Bessemer grade. The pits are distributed across a horizontal stretch of 100 feet at Fisher hill and 250 to 300 feet at the Burt lot. They dip about 25° westward, and are therefore something like 4o feet apart’ vertically at the former and 115 feet at the latter. ~Phenesaseuae marked horizons of ore within these limits. At Fisher hill the workings are 600 or 700 feet down on the incline, and at the Burt lot, 300 or 400. The railroad has been dismantled for 10 years past and the mines have been allowed to fill with water. It is quite possible that the Fisher hill and Burt lot ores are a reappearance of the Barton hill bed after a lean interval, and that they .mark a northerly continuation of-the latter Iticeyes, natural to infer these belts and especially are we prone to do so in so far as the time-honored sedimentary conceptions of origin influence us. The northern pits are double to a degree not shown by the southern, and if we are influenced by the igneous views, we may not feel justified in inferring the identity without proof of the connection. The wall rocks are practically identical and the general dip and axial trend of the pods correspond. To the east of Fisher hill and a half mile away upon the eastern slope of a different hill is another great lens or pod now known as the Smith mine, and actively worked by Witherbee, Sherman & Co., through the Cook shaft. This pod was discovered by the needle. It does not outcrop. It dips west and pitches south like the others and furnishes a non-Bessemer ore much like Old Bed, but lower:in phosphorus. A vertical shaft taps the upper end of the pod and then from the foot the two skipways fork and proceed southwest, one going for about 1000 feet. The ore varies from 20 to 40 feet thick, and at the south drops over 600 feet below its high point on the north. At the southern end is the old O’Neill shaft, now used for pumping and in the fall of 1907 tapped by the northern workings. ; Two hundred feet or so north of Cook shaft, is the Thompson, long abandoned, and beyond this an interval of some distance with no workings. Recently diamond drilling has, however, revealed ore, which may in time be worked. The hill then abruptly drops away to a small valley, on whose northern. side are two old mines, the Hall and the Sherman, which were early discovered but which | have long been idle. The property has passed to Witherbee, Sherman & Co., and has lately been drilled. Ore has been found QOgI Ul JAT}OR UdYM SOUL [JTF] JOST 61 93e[q SS Fig, 27 vu NaN) EN \ SOND -=- 4. be BN SN ONS Oe Sections 23 and 24 of Oid Bed ore bodies, Mineville. See figure Igy 122 NEW YORK STATE MUSEUM in rocks the same as at Mineville, and constitutes a reserve for the — future. It is natural to consider these last mentioned beds the northern extension of the Smith mine, and it as representing the Old Bed group, farther east and lower down than the Barton hill-Fisher hill-Burt lot series; but inasmuch as the O’Neill shaft is over a mile from the last exposure of the Old Bed series with almost no outcrops between, and in rocks that are practically massive, one may quite as well regard the northern ones as totally distinct ore — bodies. Again one’s train of thought is necessarily influenced by the sedimentary or igneous views of origin. The axial trend of the Smith mine is parallel to the same feature in all the others to the south, and therefore shows the’ same great structural char- acter, presumably due to folding, whose compressive strain being — at right angles to these axes, operated in a northwest, southeast direction. Geological relations. Up to the time of the appearance of the writer's paper on’ “ The Geology of the Magnetites near Port Henry, N. Y., and Especially those at Mineville,” in the Tvans- actions of the American Institute of Miming Engineers, 1808, volume 27, pages 146-204, the wall rocks of these great ore bodies had been generally described as “ gneiss,” and had been with entire justification regarded as the usual run of these ancient meta- morphics which habitually contain the magnetites. By mapping of each outcrop and parallel observations underground and by micro- scopic determinations it was shown that there are several dis- tinguishable types of gneiss present, and one intrusive gabbro. In the “Old Bed” group, ‘of which the: “ 21°” mine is the yclitcmume hanging wall is a very light colored acidic variety which was called the “21 gneiss.” It is a granitoid aggregate, consisting essentially of microperthite and quartz. With these and in subordinate amounts are plagioclase, magnetite, titanite and zircon. Of the last named magnetite is the chief, and often the scattered grains might easily give the observer the impression that they are some dark silicate. - Still, were a stray crystal of the emerald-green pyroxene also to appear, it would not be surprising, although one is rare. An analysis of the rock is given on pp. 49 and 50 and a recasting for its mineralogy. Additional study of many drill cores, and further observations in the mines have served to corroborate the above determination. ELIZABETHTOWN AND PORT HENRY QUADRANGLES 123 The great ore body lies beneath a cap of this very acidic rock. The ~ “ 21 gneiss” appears at times at other horizons in the series but it is not always accompanied by ore. It is moreover very similar to the wall rocks at Hammondville, if not actually identical with them. Beneath the ore appears a more basic variety, rich in hornblende, augite, and sometimes in biotite. Plagioclase is abundant and inas- much as massive gabbro is seen beneath the Barton Hill ore, the basic gneiss was believed to be a metamorphosed representative of it and ee called * gabbro-gneiss. ” Fig. 28 Old Bed ore. The black is mag- Meantime, however, we have netite; the stippled mineral is apatite; the ; lined mineral is emerald-green pyroxene. learned much regarding the syen- Actual field 0.1 inch, itic series of the Adirondacks and have also obtained some thou- sands of feet of drill cores not previously seen. From the latter it is evident that representatives of the former are the chief mem- bers in the series. Many more slides of the supposed “ gabbro- gneiss*’ serve to ally it with basic developments of the syenite series and it is much more defensible to consider the ores as lying Detween the two extremes, an acidic and a basic, of the great Syenite series. In the basic we find so much microperthitic orthoclase that it is practically impossible to draw sharp lines of distinction among these varieties when starting from the normal syenitic type. In the early paper a band of acidic gneiss was identified in the hanging wall of the Barton Hill group, and was called the “ Orchard gneiss” after one of the pits. The rock was composed essentially of quartz and plagioclase with now and then a few magnetites and zircons. One related occurrence had microcline. This must be regarded as essentially a phase of the “21 gneiss,’ since in the _ one case the albite molecule crystallized as spindles in the ortho- clase, yielding microperthite, while in the other it combined with a little of the anorthite molecule to yield oligoclase. The Orchard gneiss is soon succeeded, as one ascends Barton hill, by a darker variety containing microperthite as the most abundant mineral, with quartz, oligoclase and orthoclase as the other light colored com- ponents. The dark minerals are brown hornblende, emerald-green augite and rarely hypersthene. Apatite and magnetite are also 124 NEW YORK STATE MUSEUM present. ‘This was called the Barton gneiss. It is obviously the characteristic syenite of the Adirondack area as repeatedly described in later years by Cushing, Smyth and the writer. The additional study of the drill cores but serves to confirm its abundance in the series. lying below the Barton Hill ore body and between the Arch pit and the Lovers pit, is a goodly exposure of typical basic gabbro, so that there can be no doubt that this rock is represented in the hill i an important way. Exposures are fragmentary because of the ever present glacial drift, but the typical and unmistakable gabbro is succeeded as one follows along to the north, by a dark, basic and at times garnetiferous gneiss, which one might naturally and with great reason regard as a metamorphosed form of the gabbro itself. This was the-view taken in 1898. Repeated and painstak-— ing study of the exposures since then, and due consideration of the basic phases of the syenite series and of the character of the feld- spars, which are largely orthoclase, have led to. the conclusion that this basic gneiss belongs rather with the syenites than with the gab- bros, and that the gabbro as seen is a separate intrusive mass. Yet it must be said that there are very puzzling things to be seen. Thus as one follows along the foot wall of the ore above the Lovers pit and toward the South pit, there are exposures of dark, gneissoid rock, apparently basic syenite, yet with many little garnets like the gabbro. Again beyond this point there is rock which is believeti to be true gabbro as mapped in 1898. Yet as to the shape of the gabbro intrusive mass, no conclusion could be reached. It is in- volved in the basic gneiss, and so poorly exposed because of drift, that it is very easy to begin to speculate as to whether a mass of absorbed limestone might not locally change a syenitic magma into one gabbroic in character. Practically the same relations, equally puzzling in character, appear on the summit of the hill above the Smith mine, where garnetiferous basic (syenite) gneisses are again associated with gabbro in a very obscure manner. In the close observation of this hillside below the Lovers pit, the writer also happened on what appeared to be a small dike, about 10 inches thick, striking with the schistosity of the basic syenitic gneiss, but cutting it on the dip. It is a quite acidic rock, and re- veals in the slide, quartz and orthoclase as the most abundant minerals, less oligoclase, and a few shreds of dirty green horn- blende, so molded around the other minerals as to suggest either crushing and dragging or secondafy crystallization. There is a BaZABETE TOWN AND PORT HENRY QUADRANGLES 2s «! little magnetite and a stray zircon or two. The rock is much more acidic than the walls within which it is found, but its mineralogical affinities with the acidic phases of the syenite are close. It seems inconceivable that’ a little dike should occur alone, but no other eruptive masses have been detected with which to con- nect it. | Pegmatites. The ore bodies ate occasionally cut by pegmatite dikes of a very coarse character and of interesting mineralogy. They are chiefly quartz and orthcclase, although oligoclase enters also into the aggregate. In the walls of Old Bed pegmatitic de- velopments are characteristic of the edges and limits of the ore body and contain also coarse hornblende and large, coarse crys- talline magnetite. They seem in some way to be associated with it in origin. In the “21” pit streaks of; pegmatite run parallel with the general foliation and again give the impression of having been intimately anvolved with the ore at the time of formation. Allanite appears at times in these pegmatites and presumably from these or from others somewhere in this pit, Prof. James Hall obtained a Superb crystal which was formerly in the collections at Yale Uni- meet anda, 2. S. On a Crystal of Allanite from Port Henry, eee Jour. Sci. June 1684. p. 479]. Ten years or more ago, in mining below the present floor of the “21” pit a large pegmatite vein or dike or mass was encountered, whose relations to the ore are not accurately known to the writer. Many tons of it were thrown on the dump and it was found to he rich in zircons, at times of rather large size and of great perfection. Much less frequent arsenopyrite also appeared and one specimen of a black coaly mineral, obviously one of those containing the rare earths, but not sharply determined. In this mass of peg- matite allanite strangely enough has not been detected. Magnetites of the familiar lamellar growth, with layers parallel with the octahedron faces, are abundant. In the lower workings of the mines on Barton hill pegmatitic bodies of very interesting character have been encountered, some of which are now exposed in the new tunnel, which will further develop these lower lying ores. One mass of white fluorite with magnetite disseminated through it is cut by the tunnel and en- tirely forms one wall for a sufficient distance, to raise the ques- tion of its utilization. In other places in these workings white quartz and disseminated magnetite appear of obvious pegmatitic affinities. On the dumps of the North pit, scapolite enters into other pegmatitic lumps whose exact source in the old workings is 126 NEW YORK STATE MUSEUM unknown. In a similar way large red garnets were at one time revealed in these same pits. | ‘In the Smith mine, however, and from the Cook shaft which taps the northern end of this ore body, some of the most interesting pegmatite has been revealed. It consists of very coarse quartz and feldspar, with which allanite in irregular crystals up to the size of one’s hand is richly disseminated. Rarely good terminations can be obtained, but the mineral is so brittle that it can not be freed from the matrix except by the exercise of great care [sce Ries, H. Allanite Crystals from Mineville, Essex’ County, N. Y. WN. Y. Acad. Sci. Trans. 1898. 16:327-29]. The dump is chiefly the product of early mining, although some pegmatite has come oun im 2 carloads of recently excavated waste rock. These pegmatites and their associated minerals, some of them at least unusual in this abundance, are strongly suggestive of igneous phenomena and to the expiring stages of some intrusive mass they would naturally be referred. If, as seems most rea- sonable for Old Bed, “21” and Barton hill, we connect them with the ore, they must mark an attendant phase of its separation. Other- wise they must have come from some separate intrusive mass at a greater or less distance and one which it is not easy to identify. The basic gabbros would suggest themselves. One can scarcely attribute the pegmatites to regional metamorphic processes. Revision of local geology. The geologic map here given shows somewhat different relations in the Barton hill area in regard to the distribution of the gneisses and gabbro than were shown on the map published by the writer in 1808. It also introduces the syenite series as embracing the several gneisses called “21,” “Orchard” and “Barton.” The syenite series has been described on earlier pages, with analyses and calculations of mineralogy, which will serve to make the significance clear. As stated in the general discussion of the syenites, the ores are regarded as basic segregations in an eruptive mass of this character. Origin of the ore. In all our work hitherto the gabbros have been believed to be the latest intrusive of the larger masses. That they penetrate the anorthosites as dikes is certainly true, because among others the great dike at Avalanche lake — at the source of the Hudson — shows these relations. As against the Grenville series they are also believed to be intrusive, although decisive con- tacts are not so clearly shown as with the anorthosites. But since the anorthosites are known to be later than the Grenville and older ELIZABETHTOWN AND PORT HENRY QUADRANGLES ey than the other eruptives, there is no doubt that eruptives which cut the anorthosites are themselves later than the Grenville. When we come to the relations of the gabbros to the syenite series, especially in the vicinity of Mineville, there is much obscurity. When field work was first done by the writer in this area, the syenites had not been recognized as such, and the rocks, which we now believe to be embraced under them, were called hornblende- gneiss or augite-gneiss. In these gneisses the gabbros when dis- covered were believed to represent intrusive masses whose bound- aries, because of lack of exposures, could not be delimited or discovered. They were so involved with hornblendic gneisses that the latter were believed to have been derived from the gabbros. But as already outlined very careful revision of the exposures along Lake Champlain and on Barton hill, coupled with close microscopic study of the drill cores, has shown the following relationships. From the normal aggregate of feldspar and augite or hornblende, or, less often, hypersthene, the feldspar predominating, the syen- ites develop into basic bands in which the dark silicates are in ex- cess. .Yet there is no marked difference in kind of minerals, only a change in relative abundance. Garnets also appear, though not frequently, and the rock becomes indistinguishable to the eye from somewhat gneissoid derivatives .of the gabbros. In the writer’s former paper? gabbros were mapped on Barton hill near the Arch pit and again farther north near the Orchard pit. Between these exposures of undoubted and typical gabbro there is the stretch of dark basic rock, which we also associate with the syenites. Careful study has failed to show any recognizable contacts between the two, or more than a gradual transition. One can not say where the one ends and the other begins. Either the basic syenitic phases develop at times into gabbros, possibly by infusion of limestones trom the Grenville or else the gabbros have been in some places metamorphosed to hornblendic rocks indistinguishable under ordi- nary examination from basic phases of the syenite. In the belief that the basic gneisses beneath the ore represented the gabbro elsewhere seen in the foot wall in its massive form, the writer developed in the former paper the interpretation of the ore as a contact effect of the intrusive gabbro. In the present paper the immediate wall rocks of the ore bodies have been consistently described as members of the syenite series. With this change goes inevitably a modification of the earlier interpretation of origin. 1Am: Inst. Min. Eng. Trans. 1897. 27:146. 128 NEW YORK STATE MUSEUM Rather than contact developments along an intrusive mass of gab- -_ bro, they have been spoken of as basic segregations in syenites. . Both these interpretations are opposed to the still older belief that the ores are of sedimentary origin and the question may be perhaps stated with the arguments pro and con at this point. It is the more appropriate because among those actively engaged in mining and widely also among geologists having occasion to deal from time to time with other magnetite bodies in the Adirondacks, the rocks and associated ores are regarded as sedimentary in origin! The writer while favoring the igneous conception disclaims any personal bias toward it, other than that it has seemed to be the simplest and least objectionable interpretation of rocks, confessedly puzzling. The ores do certainly imitate to a marked degree the folds and similar structures of the stratified rocks, with perhaps this qualifica- tion that the folds are of an extreme type, being overturned, stretched and doubled up together in a very violent way. If sedi- mentary they must have been folded under such extreme pressure that the rocks flowed after the manner of viscous materials. In no other way could the Tefft shaft ore body have been pinched away from the main mass of the “21” pit. These folds are undoubtedly not essentially different from others well recognized in regions of metamorphosed, sedimentary rocks. _ The cross sections of the Alps for instance show many cases of the same sort. On the other hand if one imagines a molten magma, differentiated into layers of contrasted composition, layers which range from acidic extremes to basic, then squeezed into folds either while yet viscous or after consolidation, the result would be the same. ‘That this differentiation takes place in magmas is one of the growing convictions of students of eruptive rocks. It is certainly well enough established to justify giving it serious consideration. It may perhaps not unjustly prevent us from taking the sedimentary nature of the rocks as positively established because of the folded structure. oad Another feature which has been esteemed proof of the sedi- mentary origin is the persistence and faithfulness of the ores in stratigraphic position. In the case of the Barton Hull group, they certainly do extend as much as a mile on the strike and are persistent for this distance. If we unwrap the Old Bed group from its folds and reconnect the faulted blocks they will extend, 1See for example. W. L. Cumings, “On Sedimentary Magnetites.” En- gineering and Mining Journal. July 7, 1906. p. 25. i ‘ * ‘ ; ‘ ; ; ; ; q 1 i? 1 Fa ere Fe ELIZABETHTOWN AND PORT HENRY QUADRANGLES 120 in one dimension at least over half a mile. This is certainly on the face of it suggestive of sedimentary stratification, but in fair- ness we might say that it could also be derived from a persistent. differentiated layer in an igneous magma. It is of itself scarcely conclusive on either side. Another feature is the podlike distribution of the ore, affording its swells and pinches, and its tendency to a shinglelike distribution of the larger ore bodies. This structure is most pronounced in the Barton Hill group and is less evident in the Old Bed series. which, as thus far developed, are more like one enormous folded pod. As long ago as 1881, the relationships of ore and lighter minerals in the tailings of mills, which were engaged in concen- trating iron ores. by wet processes, impressed H. S. Munroe! as imitating the lenticular shape very clearly and the same relationship bas been noted by others since. The concentrated black or mag- netite sands, which we not infrequently observe on beaches and along rivers draining areas of magnetite-bearing rocks, are likewise suggestive. They have given much support to the sedimentary view, and it is not so clear that heavy layers of eruptive origin would assume these forms, unless compressed strongly while still viscous. It must be admitted that while not perhaps conclusive, yet the lenticular shape does accord best with sedimentary depo- sition. Another consideration, which must be emphasized in the inter- pretation of the rocks, concerns their mineralogy and their paral- lelism with other known cases. There is no doubt that the most abundant rock in the cores has exactly the mineralogy and the texture of the syenites as elsewhere identified. H. P. Cushing has shown these syenites to be beyond question intrusive in their nature. They contain fragments of the Grenville series, undoubtedly caught up in a molten mass. They present irruptive contacts with the anorthosites, penetrating the latter in dikes and tongues. Their mineralogy is essentially that of the eruptive rocks, the augite and lrypersthene especially being foreign to the metamorphosed sedi- ments. While the ores are often intimately associated, especially with the very acidic phase, described above, and while both these varieties differ from the normal syenite, yet they are so involved with it, that it is quite impossible to believe that they are sedi- mentary and the syenite eruptive. They all hang together in one. essential whole or entity and it is almost impossible to regard one 1School of Mines Quarterly. 1881. 3:43. I30 NEW YORK STATE MUSEUM as different in origin from the other. The syenite has practically — 4 convinced the writer that being igneous itself, it carries inevitably into the same great group of rocks all the associated rocks, whether they consist of acidic, or basic silicates or even of ore itself. Hence this consideration is esteemed of greater weight than the coin- cidence of the pod or lenselike shape with undoubted sedimentary structure, and, in the interpretation of the nature of the ore bodies, the preference is given to igneous processes. If we grant for the moment that the ores are of igneous origin and endeavor to understand the possible causes which have led them as well as the more basic and the more acidic phases of the syenitic rocks to form, we find ourselves confronted by great ob- scurity. It is believed by many that some sort of segregative process leads to this separation, just as pots of nickle-copper matte reatrange their composition in a fairly constant way in the few moments of cooling; or as pigs of base bullion, homogeneous when | : molten, are diverse when chilled. Some kind of physical-chemical force must assert itself and produce the variation. In connection with igneous iron ores, whose common mineral magnetite and its associated apatite are the first components of a fused magma to crystallize, many have thought that these two, being heavier than the magma, have settled out by gravity and have become concen- trated as soon as developed. Subsequent flowage might then drag them out into bands, and rearrange their position with regard to relative depth. It is interesting to note the occurrence of the ores immediately beneath very silicious layers at Mineville, but the siliclous or “21” gneiss as it now stands does not represent suffi- cient normal syenite to have yielded the vast quantity of magne- tite now found in the ore. The separation must have taken place elsewhere. In a viscous flowage, it is conceivable that the bulging folds might have been yielded under pressure, and some of the difficulties afforded by such extreme local folding of sedimentary — rocks may be avoided. In June 1909 in the American Journal of Science, page 421, F. E. Wright and E. S. Larsen published a very interesting and significant paper entitled “Quartz as a Geologic Thermometer.” The point of importance is this. When silica crystallizes above 80c° C. tridymite is the form assumed, but when it crystallizes below 800° C. quartz is the result. Furthermore when quartz develops between 575° C. and 800° C. it assumes one division of the hexagonal system (apparently the trapezohedral-hemihedral) ; while the quartz which forms below 575° C. falls in another divi- ELIZABETHTOWN AND PORT HENRY QUADRANGLES Toa sion (the trapezohedral-tetartohedral). As a result of these dif- ferences, certain contrasts of physical and optical properties arise which cast light upon the temperature at which any individual “quartz has crystallized. Experimental tests have shown that the quartz of veins and pegmatites is prevailingly of the variety below 575. C., while the quartz of granite and related igneous rocks Delongs in the variety above this critical temperature, The two “may be distinguished by certain optical properties and by etching. As a test of the nature of the rocks associated with the mag- netites, the writer asked Dr F. E. Wright to make some trials of “their quartzes. With great kindness Dr Wright consented to do so and obtained the following results in the laboratory of the Carnegie Institution in Washington. Specimen 196A came from diamond drill. hole 1g6 in the Lower Bonanza mine and was a piece of core from a point a foot or two “below theore. A dark hornblende or pyroxenic variety lies imme- diately beneath the ore, but within a foot or two the dark silicates decrease giving the more feldspathic and quartzose specimen which was tested. Five plates were cut of which three had the char- “acters of the quartz below 575° C. and two those of the variety ‘above this temperature. Dr Wright inferred that the quartz on the whole rather favored the low temperature variety formed near Mie tcriiteal point 575° C. Specimen 196C came from the same drill core about 72 feet Below the ore. The rock was considered a typical case of the "Syenite. Seven plates were cut, of which five favored the high temperature variety, and two the lower form. The conclusion teached was that these quartzites probably formed not far from the critical temperature of 575° C. —- << — Specimen 1401 V was taken from the core of hole 140, located “west of the Harmony A mine. The hole cut a thin bed of mag- pnetite. Ten plates were cut of which five were characteristic of high temperature quartz and five of low. Probably, as in the other cases, the temperature of formation was not far from 575° C. Seven plates were prepared of the lean quartzose ore from the Nichols Pond mines described below. The tests indicated that pthis quartz had never reached 575° C. These lines of evidence are not so decisive as was hoped but at all events they indicate that the rocks have passed through quite exalted temperatures. If not positively those of igneous fusion they are none the less so high as to preclude the mere burial and metamorphism of sediments. Thus if we allow a normal increase — 132 NEW YORK STATE MUSEUM of temperature of 1° C. for each 100 feet of descent, we call form 11 miles of depth to reach 575° C. This is beyond the belief of a conservative mind and forces us to the assumption of some local- — ized source of heat, 1. e. intrusive rocks. We may think of them ore as being more or less akin to pegmatites in its formation, and of the walls as perhaps being formed somehow under the influence — of mineralizers so as to require less exalted temperature of crys-_ tallization than normal eruptives, but igaeous phenomena and — influences in some form we can not reasonably escape. , | Unsatisfactory as the available suggestions of origin may appear, — it should always be realized that we are dealing with very obscure ~ and difficult questions at best, and with rocks of great age and of © complicated history. To whatever portion of the world we turn for the results of similar studies, we find geologists involved in the - same difficulties. The best that one can do is to present a candid — statement of the case leaving for the future such further light as © the general advance of the science may afford. Nichols Pond magnetite. From 3 to 3% miles north of the Fisher hill and Hall mines, there was formerly active a small enter- — prise based upon an expcsure of magnetite on Campbell mountain . 7 keen agente, Niche Te en a mile west of Nichols pond. The principal open cut is practically 3 on the summit of the mountain so that from it one looks away to” the north across the valley of the Black river. According to J. C¥ Smock [N. Y. State Mus. Bul. 7, 1889, p. 36] operations were begun in 1845 and continued to 1850. The openings are on lots ~ 166 and 168 of the Iron Ore tract. Either at this time or lates ae concentrating mili was erected upon the shores of Nichols pond — ELIZABETHTOWN AND PORT HENRY QUADRANGLES 133 and a tramway was built across its northern end which passed eastward descending some 7oo feet in about a mile and a half to the first highway in Westport. ; The deposit is lean and lies between acidic and basic gneisses very like the Mineville succession, if not identical with it. So far as one could judge, subject to local attraction, the strike was nN. 35. Ww. true, and the dip 60° west. The section of the large and more northerly pit is as follows: I Hanging wall, typical, green massive syenite. 2 Lean mixture of magnetite and quartz, 12-15 feet thick. This is illustrated in figure 29 drawn from the microscopic slide. This association is unusual, and has not been else- where seen. Beotlielcamer mixture of the same general character, 20 feet. 4 Compact, feldspathic rock, 15 feet. 5 Lean mixture of magnetite and quartz, extending under cover. The open cut was 75 to 100 feet long, 50 feet across, and had a wall about 25 feet high at the back. To the south, on the old road to Nichols pond, is another pit 15 x 15 feet. Hornblendic gneisses, presumably syenitic are shown in the foot wall, but the hanging was concealed. Professor Smock states that the ore was reported lean and titan- iferous, but the association with quartz would make the last state- mient unlikely. Professor Smock did not visit the mine. The lean- ness and remoteness are sufficient explanations for the cessation of operations. : Gates and Noble mines: Along the easterly front of the ridge which lies between Lincoln pond and New Russia there are several abandoned pits which were formerly operated to supply the forge at New Russia. Professor Smock in Bulletin 7, page 34, places iiemeaates gine on lot No. 138 of the Iron Ore tract. No work Base been doue since 1882. Professor: Smock states, “The ore has been opened a length of about 20 rods, and in one shaft to a depth of about 140 feet, and has been found to range from 2 to 16 feet in width. The strike is north-northeast and the dip of the ore bed 60° westerly. The ore is fine crystalline and averages about 50 per cent of metallic iron. Northwest of the above described opening, and in the lower ground the Vulcan Iron Company of Boston, opened a vein of ore, which was 12-20 feet wide. The ore was remarkably fine grained. The greatest depth reached was 70 feet. The ore from these mines was used mostly 134 : NEW YORK: STATE MUSEUM in the forge at New Russia. About 10,000 tons were obtained a from the Gates mine. No work has been done in there since 1682. yam The mine was also visited by B. T. Putnam as agent for the Tenth Census in 1880. His record on page 118, volume 15 of the Tenth Census Reports, is also of interest, the more because the ob- servations of those who saw the now abandoned pits in operation, are better than anything attainable today when they are filled with water. The Gates or Putnam mine is situated in Elizabethtown town- ship, northwest of Lincoln pond and about 1 mile southeast of the ~ village of New Russia. It is on Gate’s farm, but the mine itself has recently been bought by Herbert A. Putnam, and is worked by him for the supply of his forge at New Russia, The existenceyon a vein of ore here has long been known, and about 12 years ago the Bay State Iron Company opened a mine some 50 rods north of the 1 present workings. Their pit is reported to be between 200 and 200 feet deep (measured on.the dip): It is now full of water. Work on the Putnam mine was begun in January 1880. In May 1881, the pit was about 100 feet deep, measured on the foot wall, which dips 57° to the west, and at the bottom 60 feet long. The ore varies in thickness from 18 inches along the sides of the pit to 4 feet in the middle. It will average, perhaps 30 inches. The direction of the outcrop is a few degrees west of north. A part of the ore is coarsely granular and contains granules of apatite. Before it is used in the forge it is concentrated in the usual manner. Sample no. 1197 represents the ore as =i comes from the mine, and sample no. 1198 the separated ore. The samples contained SUNioe now No. 11c8 WMeetallietamon cs oo ies eee cee ee ig er 64-14 d Pulao: soil sKeye sient er pccualn Bic POR Sra nlom 3. Gt ondyec tet BE » 0-456 0-136 Mier eat eae Vari c ere mien AE ee Pi ee dc moter ase Present Present Phosphorus in 100 parts 1rom-.*.-.-24.--.. T-055 Ona It takes about 2 tons of “ primative” ore to make 1 ton of separated ore. The Gates mine was also visited at different times both by the writer and by D. H. Newland when assisting in the field. An open cut about 20 feet wide and dipping 55° southwest was observed. | The hanging wall is a dark hornblendic or pyroxenic gneiss, and ihe foot wall a light colored granitic rock. Very much the same contrasts are thus shown as at Mineville. To the west of this and the Nigger Hill pit much gabbro appears in a series of small hillocks. | Nigger Hill mine. To the south or southwest of the Gates pit is another opening locally called the Nigger Hill, but also described _ : 4 = aie 4 . L } ry 3 j 2 4 : ea lS ELIZABETHTOWN AND PORT HENRY QUADRANGLES 135 by J. C. Smock as the Noble mine. Professor Smock records the following in New York State Museum Bulletin 7, page 34, 1880. Noble mine, Nigger Will, Elizabethtown, Essex co. Another une of the Champlain Iron Company on lot No. 136 of the North hemeriesu ttact. Ihe ore~has been opened for 150 feet, on a side Diliesom the outcrop. The vein is 11 feet wide. The ore bed was first discovered in 1825. No mining has been done in 15 years. _ Mr Newland also visited the pit pointed out as the Nigger Hill mine, but whether it is the same one as described above may be un- certain. He observed a pit 60 feet long by 30 to 4o feet wide, opened by stripping off some 6 feet and less of gneiss in order to expose a very flat bed of ore beneath it. The overlying gneiss was a basic hornblendic variety, apparently a member of the syenite series, but the underlying was not recorded. This very flat position of the ore is unusual since the dips of the gneisses are as a rule steeper. It probably chanced to be left by the general erosion at the crest of an anticline or in the trough of a flat syncline. B. T. Putnam did not visit the mine for the Tenth Census, so that no analyses have been recorded. . From some stray notes of Professor Smock there may be other ~ small openings in this hill, but if so, we have not seen them. Small pits near New Russta. The sudden fall of the Boquet river at New Russia affords a water power which occasioned the erection: and operation of a forge during the period of the . bloomaries. Ore was naturally sought in the neighborhood and apeotmer poitits than the Gates and Nigger Hill pits. A series of small beds was discovered along the west side of the valley and small excavations were made at three or four points. To these the writer was guided by Mr Frank Morehouse of New Russia. The most southerly one is the Pitkin bed which was in the foot of the hills just west of the highway about 4 mile south of New Russia. A small pit had been sunk on a thin bed of ore. Next north is the Castaline a short distance up the valley of Roaring brook and on the south side. Speaking of this and others near, Professor Smock in Bulletin 7, page 34, states, “ West of the Boquet river in this town magnetic iron ore in workable extent has been discovered on what is known as the Castaline place, north of New Russia and in the Wakefield, Post and Ross veins. Since the stopping of the forges these mines have lain idle. The Castaline is one of the oldest openings in the country. Watson, in his history of Essex county, says that ore was taken out of it about 1800 and used in forges.” 136 NEW YORK STATE MUSEUM Some small pits were located by the writer after search in the — woods, but they had long been abandoned and from them few details could be gathered. The rock in the vicinity was a basic, liornblendic variety and was considered a derivative of the gabbros, raising the question of titanium, but no analyses have been made. The Ross ore bed is in the easterly foot of Oak hill about a mile north of New Russia... There is a lower opening and an upper, perhaps 300 feet vertically higher up. The lower opening, believed to be the Ross bed, exhibits streaks of magnetite in well foliated hernblendic gneiss, while a hundred yards east and 75 feet below, appears acidic gneiss, so that the familiar Mineville section is again shown. | | The upper opening is in gneissoid gabbro with massive gabbro near. It is a lean ore 4-5 feet thick striking northwest and dip- ping at a flat angle to the west. An analysis of a sample by W. F. © Hillebrand gave the following [U. S. Geol. Sur. 19th An. Rep’t - 1899, 3:408]: : TiOs Pe rk oe eR ren EOL As Gc ay St ce en Pee Oia ie aie ees Cates ke es et a a eee Ie ee ae 22.01 Fe.O; wane alte ae Loca Pinta nt ps ll arn akira ce ak Alon ee eR 30-34 SiO pe eo rae ae Sa Pee A ee, Seep ee ir pe eens ce at He AL Opn 2s ee ee ie Bi SEE Eee ee ecu eg ee 708 Ohh © MAIN e omens ee antes ua s ota SR acne alors gts SB th enetn A Tn 3 none OLh © er ree ERR ye Ue mn Lice Tbe Arn tay I ee 2e7R@ MgO Le alo tes aries Spee cal, Foe ne GeO Tg EE OAD Reese: BARE gaa Nein et Ne cee Ae SPR 6-92 Ks ie i ae Ee Se RR ea ee ee pes pees iy hn ee 0.41 DY © aerate ns emer oar tre Geman Tet ree O. 53 De i © eee ican a ARP Mae ch il edt ah vagy ars ad age ice oda Pucwelbme eure 0.95 At) © tage Aces Se RN NAA Heir Uh sa ae SM ans a uae mn Soa 5 vii i Oe a ae are ae 2 9 TS ene OM IG RE Ae CS tena 0-04 COB ee SS EN SN oc SR Re Ode EE ats ae 0-42 COs Eis Sa Ee SFE BRAG Bete ee pt re nee ee trace (CER SS ics a eae es een ap AB tee ee I ee Re ee ee ‘trace BY ig aipeemes aera creo em nt er Pate gine wal es Seren ond Bera Senee ee ieee en fit a trace Eta a re ee OE Site ee ees eevee is Se Cos re GO Si fy tart e grha te Ve Un eee RM ce Reus PER ME a rae De Ne re. 1S eh A NGh Deer get es 38.98 This ore is not very high in titanium but it really belongs in the group of the titaniferous magnetites which will be taken up sep- arately. It is curiously high in chlorin, leading one to suspect the presence of scapolite, since the apatite is obviously too small to care for it. ; Steele ore bed. Aside from the titaniferous magnetites this is the one remaining occurrence met within the area. It is situated ELIZABETHTOWN AND PORT HENRY QUADRANGLES eS about a mile southeast of Elizabethtown village and is exceptional in having a thin bed of limestone of the Grenville for its hanging wall. The pit was filled with water so that the lower edge of the ere was not seen. The exposed face was cut by a small fault which is illustrated in figure 30. The ore is a granular magnetite, I Limestone ZA Fig, 30 Cross section of the Steele ore body near Elizabethtow>. and has an apparent strike northeast with a dip west. In only one other instance has ore in or next limestone been noted in the eastern Adirondacks and that is the Weston bed, near Keene Center. Limestones are not far, however, from both the Cheever Pcie ePiicrsuire beds, im each case in the hanging. b The titaniferous magnetites The interesting mineral deposits of this character are more nt- merous in the Elizabethtown and Port Henry quadrangles than elsewhere in the Adirondack region, but they are individually not me datee Mor as tich in irom as are those near Lake Sanford, at the headwaters of the Hudson and in the Santanoni quadrangle. The geological associations are also different. The Lake Sanford bodies are in the anorthosites, whereas, the ones here specially treated are in the basic gabbros. So far as our detailed explora- tions have gone, the basic gabbros seem to reach their greatest de- velopment in the area covered by the two quadrangles here described and extending a short distance north and south. Through- out their many exposures the titaniferous magnetites occur rather frequently and while at present not possessing commercial values as sources of iron, they are of much scientific interest. The basic gabbros in this section favor the borders or general 138 NEW YORK STATE MUSEUM contact belts between the anorthosites and the other rocks to the eastward. They form irregular masses of a square mile or less @ in area, and have revealed few details which would enable the — observer to describe them as laccoliths or intruded sheets, or stocks. ‘They certainly do appear in dikes, and the larger masses display 4 characteristic irruptive contacts with the older rocks. 3 The bodies of magnetite or of intermingled magnetite and il menite are merely phases of the gabbro, exceptionally enrichedaam with the iron-bearing minerals. There is no sharp demarcation between so called ore and rock. All the rock has some ilmenite- magnetite. All the ore? contains some of the common minerals of the rock, viz: olivine, pyroxene, and garnet, but the feldspar tends tc fail. Weare compelled therefore to regard the orem) oates simply as basic phases of the gabbro, exceptionally enriched with cne of its normal minerals. Details of these relationships will be brought out under descriptions of the individual ore bodies, of which some 10 or more have been discovered. ~ In canken yeaus much attention was directed to them and in at least four instances they have been opened on a scale which has left pits and tunnels of no small size. In one instance, the Split Rock mine; a magnetic mill was built in the hope of reducing the titanium. The several deposits will be taken up from north to south. so as to begin with the best known and most developed case. Split Rock mine. From Westport to the northeast the shores of Lake Champlain are formed by a rugged ridge, known as Split Rock mountain, from the rocky islet which is, as it were, split off from its extreme point just beyond the limits of our map. Toward Lake Champlain it is precipitous and rough, forming a general fault scarp with many picturesque reentrant bays where cross faults intersect the master one. The summit of the ridge is very irregu- lar but the northwestern slope is more gentle. On the precipitous eastern front and some 5 miles from Westport a mass of titanif- erous ore is exposed at a point about 100 feet above the water. It attracted attention about 40 years ago, and as it stood in a position — 4 very convenient for mining and shipping it was opened up on a fairly large scale. Boarding houses were built in a notch in the. ridge just above and in the end a mill was erected at the shore of the lake. A road leads out to the westward to the highway as shown on the map. 1The word ore is here employed in its purely scientific meaning as implying the richly metalliferous minerals; not in its technical sense as capable of being produced at a profit. ELIZABETHTOWN AND PORT HENRY QUADRANGLES 139 The ore occurs in a moderately large mass of gabbro which can be traced in the vicinity. It is a dark green or black rock, con- sisting of augite, hypersthene, brown hornblende, garnet, original basic plagioclase, charged with pyroxenic dust and minute spinels, secondary plagioclase in clear rims around the last named, and of the magnetite-ilmenite mixture. The ore is 10 feet or more thick, and forms a flattened body, which strikes into the hill n. 70°-80° e. and dips 50° south. An open cut has been excavated 30-40 feetecdeep and 25 feet high. From ‘its mouth the old dump of broken ore streams like a talus down to the lake shore. To the south another small opening is reported but this has not been vis- ited by the writer. While the rock mass is faintly foliated from dynamic effects, there is no sharp transition from ore to rock. The former is simply a basic phase of the latter and the exposures are so good that this locality is a specially favorable one for the study of the relations. © | In cracks through the ore a curious isotropic green substance is somewhat rarely found which contains some dusty magnetite and the decomposed remains of feldspar crystals. It has been pre- viously described by the writer as a glass, but its identity can not be sharply determined without a quantitative chemical analysis. Its specific gravity is 2.822 which is higher than the common iso- tropic minerals which might occur in these relations. An analysis of the wall rock has been made by W. F. Hillebrand and also one of the ore, nos. 1 and 2 below. No. 3 is an analysis by George W. Maynard, made in the early seventies. Nos. 1 and 2 are from the 19th Annual Report of the United States Geological Survey, volume 3, page 402; no. 3, Journal of the British lron and Steel Institute, volume 1, 1874. I 2 3 PRE i SR A 47.88 17-90 16.46 Isso SoA noite ocncel a. a(S ele Soe a 3 1.20 15-66 14.70 he al eR Ee i earn ttre 2 RIA ameea gear AB chic lp a Se Re ee 18.90 10.23 34 UN eS Ph ae te sages « behead’ eo) 15.05 38.43 CMC EE et coh ch nie a's, es cep ee oles 10-45 ° 27.904 23-40 MING Se Sie ses teeta < Gad Serene «tine -02' not. det. not det. SII Geet AE We BE Se ook i PN RG iDiee “23 MN em etre oT seo ay aay ow 0.8 7.10 6.04 ZEN: MORE Aer eed oe AES se 5b cuPodone «oss! 8. 36 2.86 3-54 a Se ed Ea Pia ts a ee [MOS enttoecan imbue Mention cc T40 NEW YORK “STATE MUSEUM K,O aN aNidhaat abies SPA aan SS nee ean ee ane IST. notadet: --o-eemee Nias) FS ac Bes eee oe re ae 2.75 . not det. +... eaee Testy cercecte se Se as Dee ee eee pene eee ae (i. «eee eee EN © ar i ei er ia ears Renee, ee (Ro ee ke eee EU Ore. re ae Seek Ei pits a) sek 43 1+ 33) eee UBS © Peperr dere reagent tect ance etn ingot Bie .20 04-4. nee Es @ aan e aerinl ee nett rar men ee cen ial, 2°. mh (tins 55 cee ee Ory cheno ae eeanen OR se awe 2 ween pal ~1Os ieee oe She troy irae Cee ha ae acer eae 107, BA eee ATE dea eae ae en ad Cee a TOO: 02 99-15 QQ - 23 Pa a ae SY ke i A ee 322.82 22550 AS) OA Grima. chiara prerey wie cemtcep cenit te ee Shoe 3-090 4-128) eee When recast the above analyses yield the following percentages which are approximate but unquestionably near the truth. No. 3, however, can not be recast with so great an excess of Fe,O, over Fe@Ou I 2 iMiisalsnahur meena ge eto nra ee sincere mys yt or en Ge ry) 29-42 Ma onerite it se siinthe Dosa- lane, order 5, Germanare, rang 4, Docalcic, Hessase, subrang 3, Persodic, Hessose; no. 2 falls in class [V Dofemane, order 4; Domitic, Adirondackare, suborder 3, Tilhemic, Champlainiore, rang i, Permirlic Champlainiase, section 1, Permiric Champlaimiose These last names will suggest the large part that the Adirondack titaniferous magnetites play in the nomenclature of the system. Ledge Hill mines. About 2 miles a little south of west from the village of Westport an abrupt hill rises to a hight of 1140 feet. On the northeastern side and a short distance below the summit two- pits have been opened upon masses of ore in the gabbro. The ore ELIZABETHTOWN AND PORT HENRY QUADRANGLES I4t in one pit has a long dimension in a northeasterly direction and has been exposed in a cut 75-100 feet long and 30-40 feet deep. The second mass has a pit about 25 by 8 feet which is entered by a cut | at right angles to its long dimension, and 15 by 15 feet in size. The pits can not be far from the goo or 1000 foot contour. The wall reck is typical gabbro and while no analyses have been made of the ore, it has all the associations of the titaniferous varieties, is dense and characteristic in the specimens and is believed without doubt to belong to this variety. The name “ Ledge hill”? may not be the best one but it was given the writer in early work in the region. The locality is in lot 163 of the Iron Ore tract. The notes upon the pits were first published in Bulletin 14 of the New York State Museum, page 350, but the openings were again visited in 1907. In the southeastern foot of this same hill; approximately on the 700 foot contour, and a short distance from the highway, there 1s another small pit in a very basic, hornblendic gneiss. Lean, dense magnetite is exposed which is apparently titaniferous. It is a small pit and no analyses have been made. | The remaining occurrences of the titaniferous ores are in Eliza- bethtown and Moriah. Tunnel Mountain mines. The Black river heads in Lincoln pond in the southeastern portion of Elizabethtown and thence flows east of north through a wild and narrow pass in which was formerly located the old forge and little village of Kingdom. The relations both of the pond and the river are now somewhat changed from those depicted on the map, because of the damming of the river a few years ago and the erection of an electric power plant for the mines at Mineville. The pond is much expanded and the © roads have been somewhat changed. At the point where the river begins to form the boundary between Elizabethtown and Westport, it rounds the foot of an eminence on the northwest, which is called Tunnel mountain, from an adit which was run many years ago near the Summit. It was intended that the adit should tap a large body of ore which outcrops higher up. At the eastern foot of Tunnel mountain, two small pits have been cpened which at the time they were visited were on land belonging ‘to John Tryan. The first was 15 feet square by 10 feet deep, and in lean ore which gradually shades into wall rock. It contained inuch biotite. A thin section revealed titaniferous magnetite, olivine, brown hornblende, deep brown biotite, garnet and clear, 142 _ NEW YORK STATE MUSEUM unclouded plagioclase. The biotite is closely involved with the — particles of ore. A partial analysis of the so called “ore” by W. F. Hillebrand gave the following: LEhCes © ene Marts rae: 3 4 TiOs TOR Ss V205 3453 Stor Mes Os aren vac Les CroO03 2215 P2O5 .46 Fe 24.05 The specific gravity was 3.199. The above percentages corre- spond to LDR cesa lt miPGeen ge te ee Rema aE eh ar Catt ES 3 8 eed Bais G =) BE Serial Wao inetitie fess 5: i tegen cee auch ae ae rene nes ae 16.704 RenraininesHe@) oo. accueics Seas eee ee ee eee 6.912 The association with biotite is unusual for the Adirondacks but has been noted in: Brazil by O. A. Derby [Am. Jour. Sci. Apr. Hoo 7 s 311]. ee hundred yards northwest is another pit 15 by 30 feet and 10 feet deep. The walls are gneissoid gabbro and the ore resembles the usual run of the gabbro ores. No analysis has been made, but the specific gravity of 3.964 indicates more iron than the aes from the first pit. At the extreme summit of aie mountain which stands at 1640 feet a mass of ore outcrops, larger than the bodies at the foot, and indicating from its position a character of exceptional resistance to erosion and weathering. An open cut has been excavated 40 feet long, 10 feet wide, and. apparently 40 or 50 feet deep. It is now filled with water and its depth is estimated by the size of the neigh- boring dump. The cut runs north and south and is parallel with the vertical foliation of the walls. Lean ore and gabbro (or strictly speaking norite) outcrop 10 or 15 yards to the west across the strike and gradually pass into the usual massive rock. Some 200 feet vertically below the summit and south of it, in the side of one of the characteristie cross gulches of the mountains an adit has been run with the intention of striking the ore in depth. It must be roo to 150 feet long, and while it seems not to have cut the ore, it has yielded beautifully fresh samples of the country rock, besides giving the name to the mountain. When examined in thin section, the rock proves to be a true, gneissoid norite, hypersthene being the most prominent bisilicate present. It is thus analogous to the basic rocks of Norway which contain titaniferous magnetite in that country. Green augite, brown horn- ~ biende, plagioclase and garnet are the other components. In the ore, the microscope reveals besides the iron minerals, brown horn- blende, serpentinized olivine, garnet and colorless transparent labra- ELIZABETHTOWN AND PORT HENRY QUADRANGLES TAS dorite. An analysis of the ore by W. F. Hillebrand gave the fol- lowing results: Slo: 2a (Pe) Gea A oo © PRE Serre ec ACE es ee .02 oor 5 ee 16.45 See ARE pa ATE eres ee bale -09 EON Ie eerie | MC eerne bec ous cen oe a Pe oma present Ci5©: Pees ee te es a saa slg etruletare ens, eas cane ae mae iae: ti lel 2) 26 SS eer ADL Eola a4 © er aia ay SERA Neeeia Farias 1.68 LP iO? A Tb dot Ret hae 28.82 GO ree aie en Seatcas a eed ay) (12 G8 6 A ee eee 6.63 — IUD) (2 88S Sa Fas vs A OialeMren de kk as oe 99-62 VEO (pies ea CL ee cas oec chee a ct «ahh oe B50e When recast this analysis may be split up into the following components which are undoubtedly very near the true proportions: Leen 2 ZOE SO si CalGieery mtd es ee has eae 40 Wetemietites ----..2+-...-.. BOBO We VN AES Palin oie Mere co St wae ras (CET MOMs le ViAAC TC tO: Fins Sieur 61 ATOR” eo 9-45 SS terltitaig Perec s ea eens -09 SDE Secs ae eee Fano eeP MOS MilOLisier nse fon ack es .02 Sie =-2) eee 6.94 Residue, Si@)s noe eae a ctee ete 220 Si II-4o ya RR Se | Alea re eter tee al eon ote 99-57 In the quantitative system this has the same name as the one last recast. It is probable that from the Tunnel mountain pit came the sample analyzed by Prof. George W. Maynard [British Iron and Steel inst. Jour. 1874] under the name of the Kingdom Works. He gives 7 WOR HOlor 2 went feces ere ware a ae 21-64 a oS Zl. 24 TNE G) setae ee te ete de Ir. 85 Pap ly oS See ee Baofah. NG SiO): hd aia Oar Mer Ree eter PL 2. Bl 0 87 DP Gtr eesti oc eee ce eee 96.07 1 Fe a A sae oA reg UE Mae 32.50 Professor Maynard also gives another under the name Iron mountain, Elizabethtown, but the exact locality is not known to the writer. lo: 4 Se 16.37 PSA (OS ahaa Ok MI ER tee ch, 9-35 i A RUMP MEEBO) 02 oie (eae oe 52 o tnson hom The Ge 0 a eS 30. 36 jel O iy ae aera pink Beko dtMcachin tats 13 MnO RETA CU. fee ue fey «= Ay. 08 yl IO. 26 TRO Pali caen SOL ie eee 100.13 Fe Be ieee he oh ateerace dita eee ete eee 40.42 ‘Pits near Little pond. Some 2% miles south and a little east from Elizabethtown and back from the present highway is a small 144 NEW YORK STATE MUSEUM ‘lake, known as Little pond. An old road passes it and out through the valley of Kerner brook and is reputed to be the one made by the first settlers in entering what is now Pleasant valley. A little to the northeast of the pond and in two hillocks of gabbro, openings have been made upon bodies of titaniferous ore. of considerable size. A great area of dark basic gabbro is present in these hills, and the openings have been excavated in masses of ore occurring ~ in it. ~The north pit is 20 by 20 feet and 1 feet deep. — Uitersenam pit, 200-300 yards southeast, is run in a hillside and is 30 by 30 teet. The working face is 25 feet high. The ore contains the same green isotropic substance described from Split Rock. Great ex- _pectations were raised by these ore bodies when first discovered ;: thus W. C. Watson in his History of Essex County, statesmeuau the ore forms an entire hill and is inexhaustible in amount.! . The wall rock of the pits is the usual green gabbro of this region. The ore is found on microscopic examination to contain, besides. the ilmenite and magnetite, brown hornblende, olivine, garnet, and plagioclase. The following partial analyses by W. F. Hilde- brand indicate the composition. When recast we obtain the 4 third and fourth columns. North .:So th North South pit pit pit pit Via ia ie eee TO 02) 3 Oy hee lone Tithe my sume wear 35.27 2s Re@Ouae oes: 20:78 28.35 | Magnetite .-...-- 38-05 16.24 FeE@nt setae 26-30; Tt 26 > Chnonmitem see. -64 vAG CriO eee? pie ae 7s 127) a soy ti Oreten eta ieee 18 26 VeOg Bae ieee 62 50 POR eee Res tr. 32 See eee 06 IO APO tree ema 70 282 53-87 Fe 2hek hice AL EPNOOh a -y- ose Gls | eae Say: 82 Kero ilies pers eee DO Men era Diss S .26 -O4 @aleitec cr ct eee: SOO! 4, eras 2 bee n.d. FORPSIMS DUC Mee cen ute ee cae 20a iene Guantitative system the rock comes under class. III, Salfemane, order 5, Gallare, rang 4, Auvergnase, subrang 3, Au- @erenose. he ore falls in class 1V, Dofemane; order 4, Adiron- dackare, suborder 2, Adirondackore, rang 1, Adirondackase. The above is unusually high in apatite for ore of this variety. It is also remarkable in yielding a very small amount of free carbon, as to the condition of which in the ore one can only surmise. Graphite would be the most probable mineral. Oak Hill pit. In speaking of the Ross pit upon an early page, it was remarked that an apparently titaniferous ore had been opened higher up on the hillside. The locality is approximately a mile north of New Russia, on the western side of the highway. A specimen yielded W. F. Hillebrand the following results, which have been recast for the mineralogy. The ore is low in TiO, but 146 - NEW YORK STATE MUSEUM . : it has a remarkably high percentage of chlorine, leading one to sus- _ pect the presence of scapolite, as was suggested by Dr Hillebrand. _ A trace of carbon was found in this sample recalling the results __ just stated under the Lincoln Pond pit. oe The Oak Hill pit is a small one, in gabbro like the others. Oak Hill ore Pa Qee aa are ee ae 5 2rsl. Ulaieinitieson-. 2 Orthoclase. nce eee 2922 KSO') Bae ech ren cee are Al : | Bt eG a a On ee ee ta co 5G Eta @) SP ake asetanice haem ero 95 ; PEOEPAS actiustacnan oomunereee meds -14 RAD PORES AARC Url ate Ars rite fits A - Od CLs Seteee ewer iaees eenarer -42 Rataltents ice hele ae 99.81 WY eRe Cane eth a en Na 38.98 In the quantitative system this ore has the same series of names as the one last mentioned from. Lincoln pond. Titaniferous ores in Moriah. The presence of a titaniferous body near Cook shaft, north of Mineville, but actually in Elizabeth- town has been earlier remarked. The possibility of the presence of titanium in the Craig harbor bed has also been suggested. Be- sides these, however, several occurrences have been mentioned to the writer by Mr S. Lefevre, chief engineer of Witherbee, Sher- nan & Co. Specimens have been brought in from time to time to Witherbee, Sherman & Co., for analysis, but the writer has not seen the occurrences in the field. Juittle 1f any work had@bcem done upon them, so far as known, and while in the field, they were not noted. The bodies are liable to appear in any of the gabbro areas. West of Mineville is Mt Tom on whose western side is a high- way which is prolonged in a trail to Newport pond An occurrence 1s reported somewhere near this trail. Another occurrence has been reported about a half mile due north of Feeder pond, in the southwestern shoulder of the hill reaching 1640 feet. About 2%4 miles west of Moriah Corners (or Moriah on the map), a highway turns due south, and at 34 of a mile bends sharply 7 ELIZABETHTOWN AND PORT HENRY. QUADRANGLES WA, to the east. In the hills somewhere southwest of this angle of the highway another occurrence has been reported. Commercial value of the above titaniferous ores. So much interest has been felt in the exposures of these ores that a few re- marks should be made upon their commercial values. Enough analyses are now in hand to illustrate in a satisfactory manner what may be expected. ‘The percentages in iron, titanic oxid, phosphorus and sulfur may be first summarized, with the name of the sampler. Fe TiOz ip S Seeeteciyey iP. Kemp.... 2.00... 055 82-62). 11560 -O17 it eeoeoek. G VW. Maynard..........-. 32659) Oh 14 70 ieeveiinoitet 2. Wemp....s.. 26. e ee eke 24.65 LO. 55 .20 bait) Riageemonniain, J. Fo Kemp........... 35-99 16.42 - 009 -09 meee wpond., jr. Kemp.... 0... 2. ALS 7 Vlora? if -06 wieempemid), oF. Kemp...) 2... ee le 20:67". E307 qa aks mecamepond, J. F. Kemp: 2.--..s.4..8.- GH TOU ADT - 36 -O4 eves B. Kemp. io... ees ' 38.98 Sen 06 -04 Kingdom Works, G. W. Maynard...... BANA O Male R oie wer Steel os 2 ies eh Set iioaamountan, J. EF. Kemp..... Bice as ire ueeee 7a Oi GW el MANOR 7 ists EA he eA It is at once apparent that all these ores are extremely low grade, the richest being 44.19 and only two others reaching 40. Since under present conditions and those which are likely to continue for many years, no magnetite under 50 per cent in iron,is of importance as a source of lump ore, unless it should have exceptional purity in phosphorus and sulfur, be lacking in titanium, and be in addition located near a furnace, there is little encouragement to look with favor upon bodies of this type. The percentages in phosphorus and sulfur are also munoetane features. In sulfur the ores are obviously low. In phosphorus they are variable. In instances such as Split Rock, and Tunnel moun- tain, they are very low; in others they are quite high as at Lincoln pond. There is a somewhat widely prevalent impression. that the titaniferous ores always run low in phosphorus.and sulfur but this is clearly unjustified. As with other ores each case must be sampled by itself. The presence of vanadium in these ores is a matter of much scientific interest and since the element has come into such ex- tended uSe for high grade steels some have looked to the titanif- _ erous ores as possible sources. If we summarize the results given above, we obtain: V20s | . NEO: PROC ©. hee rt ee Pe LAMCOM »POTld ein slo va area 62 Seaman it. ot ee Bare Me tele. ONC year as tise tere whe ee 50 Sitanel mountain .-...--.-> ‘ON ESYD Mee fo) 118 Went ere RC as -O4 148 NEW YORK STATE MUSEUM In just what form the vanadium is combined is unknown. From its chemical properties similar to phosphorus one would suspect some compound analogous to apatite, just as we have pyromorphite and vanadinite, but although the vanadic oxid exceeds in amount the phosphoric the mineral. containing it has never been isolated. Ferro-vanadium is manufactured from vanadium compounds by electrical processes and contains about 25-27 per cent of this ele- ment. It would appear as if the percentage of this valuable sub-. stance were too low to make it a serious factor in the value of the ore, but as the industry of vanadium is as yet in its infancy one should speak regarding the future in a conservative spirit. In vanadium steel, now so highly prized for its toughness, there is much less than one per cent vanadium. Elementary vanadium constitutes 77.4 per cent of vanadic oxid (V,O,). Magnetic iron ores under 50 per cent and not fulfilling the conditions stated above, must undergo magnetic concentration if they are to be utilized. It is with regard to this method of treat- ment that the recasting of the analyses into percentages of ilmenite and magnetite has especial significance. The magnetite would be the mineral saved and the one upon which efforts would be es- pecially expended. The iron in the ilmenite we would expect if not hope to lose, so as to reduce the titanium. The iron in the pyroxene and olivine would pass off in the nonmagnetic tailings. So far as iron is concerned we are therefore reduced to consider- ‘ing alone the magnetite and therefore the following tabular sum- mary is presented. . Iron in Imoenite Magnetite magnetite SDE BROCK Baetie tre cee ee cee nals tect . 20-42 223077 oases Spt rocks sce ve a cok eet ae eee ree 27205 2250 23.74 "EE Vert Aes ate aa ae een re cee oe nse 25.34 16.75 T22-1O Tine! ino tmntains ier see a ee 30-80 29-80 21-58 Littles, pond ok enc tac «eee ee ee 35°27 - 38-050 8 275g Little pod a. poe acne et ee en ore 2a 24-49 16.24 Eia7o Lincoln pond .. oy sinister 22-05 44-31 32-08 Oi rete ab Recenter eters eee cua RN Hpi ee 9-70" “44-087 Bison Kanedoma: WV orlks.756 ee ens ee ee eee BA OA “27208 22.50 Iron: mountain, lizabethtowms a. ieee 30:80. 35-73% 2eemm These results show that even if the ilmenite and magnetite are so coarsely intergrown as to make a separation feasible, the grade of the ore is too low to make the separation a likely source of profit. On the other hand the ore is extremely hard and fine grained, quite different from the richer and more coarsely crystal-— line occurrences at Lake Sanford and parallels can not be justly ELIZABETHTOWN AND PORT HENRY QUADRANGLES T490 drawn. While the concentrates would doubtless be somewhat en- riched in iron by ilmenite which would enter them, they would be decreased by some inevitable losses in magnetite, and by just so much as the titanium exceeded a very. small value, say one per cent, the operators of iron furnaces under present slag calculations would regard them unfavorably. The conclusion is quite irresistible that only by smelting in the crude or lump form, and by the development of a process which does not find titanium objectionable, and under conditions where ores of iron content of 35-45 could be utilized, can these deposits be made available. Regarding the smelting of these ores, the follow- ing papers by Mr A. J. Rossi should be consulted by any one interested. Jitamferous Ores in the Blast Furnace [Am. Inst. Min. Eng. Trans. 1893. 21:832]; The Smelting of Titamferous @erethe iron Age. Feb. 6,'20, 1806]. c Red hematite There is but one locality for this mineral and it is one of no - more than scientific importance. On the south side of McKenzie brook, just west of the highway running south along the shore from Port Henry, a series of pits was dug years ago upon a red outcrop which suggested ore. ‘The red color is due to hematite which has developed as a decomposition product along a line of faulting and crushing. The country rock is'a basic member of the syenite series and the fault runs about n. 70° w. nearly parallel with the present brook. The decomposition of the pyroxene or horn- blende has apparently yielded the red hematite, just as from sim1- lar causes certain portions of the richly apatitic-ore at Mineville are stained red. The present dumps along McKenzie brook dis- play very lean and greatly slickensided material and there is little reason to regard the occurrence as more than an interesting case of faulting. 2 Limestone a Flux and macadam. Luimestones for these two purposes have been chiefly quarried near Port Henry. For flux in the blast fur- maces in former years the Grenville limestones were extensively opened. They furnished a coarsely crystalline variety which was a fairly pure calcite except in so far as this mineral was mixed with disseminated silicates. All through the quarry faces streaks of hornblende schist, bunches and lenses of pegmatite, and finely disseminated pyroxenes often altered to serpentine, are present 150 NEW YORK STATE MUSEUM in such abundance as to cause much waste. From between them the purer streaks of limestone were selected and used as stock in the furnaces. The rejected dumps now furnish interesting 7 material for the mineralogist, since well terminated crystals at times project into pockets of calcite in such relations that they may be easily freed. The pure, white limestone is occasionally replaced 6 the ser pentinous variety, ophicalcite, locally called Moriah marble, -and this will be again referred to under ornamental stone. The quarries in the Grenville have been shut down for years, since, although the old Cedar Point furnace is still in vigorous campaign the necessary limestone is elsewhere obtained. The largest of the old quarries is the Pease, just north of Mull brook in the outskirts of Port Henry. An impressive face of limestone is exposed with a large black sheet of hornblende schist capping the top. A half mile farther north and on the northern side of the brook which flows into Craig harbor, 1s another opening, quite similar in geological relations. A third one lies on the western side of the ridge which separates Mineville from the lake, and is just south of the Pilfershire iron mines on the east side of Barton brook. In this last named quarry is the broken dike or sheet of hornblendic rock, shown in plate 9. There are many other places where this same limestone could be opened up if needed but at present there seems to be no call for the material. The present source of flux for the furnace is ne faulted block of Beekmantown limestone on the lake shore just south of Craig harbor. It furnishes’a somewhat silicious, magnesian variety and is broken and carted to the furnace yard as needed. Were other varieties required, the Chazy and Trenton ledges on Crown point would deserve investigation, since the Chazy on Willsboro point is a fairly pure calcite, although it varies somewhat in different beds. In a small way the Grenville limestones have been quarried and burned for lime in former years. The industry was, however, rather a feature of the earlier and more isolated conditions than those of today. The ruins of an old kiln are still recognizable — along the road to North Hudson and about 3 miles west of Moriah. Corners. Another one is in the western foot of Woods hill, about a mile north of Elizabethtown. From stray bits of clinker it is probable that one also was in existence near the ledge on the north- eastern feeders of Jackson brook. : To a small extent the Beekmantown resins from the furnace © quarry, near Port Henry, has been used for macadam, but there q z i SEIS BETHTOWN AND PORT HENRY OUADRANGLES 1S) 18 is no doubt that should road metal of this character be needed in the movement for improved highways, this particular stratum should receive careful attention. While it appears near Port Henry chiefly in the two faulted blocks along the lake, it is present in great amount in Westport, and to the south in Crown Point it covers a rather large area. As it appears, moreover, 1n the regions of the Champlain clay, where the roads are particularly bad in wet weather, it may be worthy of investigation. Being a hard and as a rule silicious variety it would seem to be best adapted of all the -local stone for macadam. As a natural material for use upon the highways the calcareous sand or gravel, which results from the surface decomposition of the Grenville limestone, has been dug to advantage. It is occa- sionally available in pockets of sufficient size to yield borrow pits of moderate capacity, and it packs under traffic to a very.excellent surface. b Limestones for building and ornament. The Paleozoic strata could furnish limestone suitable for structural purposes 1f desired, but except in the barracks of the old fort on Crown point, they have not been extensively utilized. The Chazy is the best available for these purposes, because of its heavy bedding, and more uniform character. The remains of the old Crown Point quarry can still be seen, but it has not been much if at all utilized im Jater years. ~The Beekmantown is also a rather heavily bedded stratum but is irregular in character and harder for tool treatment. The Trenton strata are as a rule too shaly for extended use. The one ornamental stone within the area here described is the serpentinous marble which appears in several localities in the Grenville series. It has also been used for walls in the village of Port Henry. The more abundant white crystalline limestone is occasionally replaced by beds which are mottled with green ser- pentine, affording when the mottling is regular and not too coarse, a very beautiful ornamental stone which was formerly placed on the market as verd-antique or Moriah marble. The difficulty in the industry is the irregularity of the serpentine, which at times is in large masses and again in small, shotlike disseminations. . There are three points at which the stone has been taken out. One, the Treadway quarry, is on the brook which flows into Craig harbor, just north of Port Henry and near the point where the fork is shown at its headwaters. A ledge 10 or 15 feet thick was here channeled out in former years but has not been worked for 152 NEW) YORI Si. 2 eM SeU wi at least 20 years past. Another quarry is mext the tigmwaye quarter mile north of the Cheever mine. A third, the Reed quarry, is in western Moriah just southeast of Broughton ledge and in the curious loop made by the brook which rises at its foot. This last named opening has been more recently worked than the others. The petrography of these rocks has been discussed in the general treatment of the Grenville. 3 Clay The Champlain clays are. very generally present upon the flat Paleozoic strata wherever these appear in the larger areas along the lake shore. The clays constitute the surface over the larger partion of the peninsula of Crown point and are widespread in Westport. Should they be needed in the future as the raw ma- terials of brick they could be furnished in any desirable amount. Up to the present the industry is practically undeveloped and these resources may be considered as reserves. It-1s probable, that like the similar clays elsewhere they would furnish a good grade of — ordinary red brick. The sand for tempering would of necessity be sought in the higher terraces along the Archean front, where the deltas and water-sorted drift contain it. Judicious search would undoubtedly serve to locate the sand and clay in proximity with each other. Chapter II : MINERALOGY The area of the Elizabethtown and Port Henry quadrangles presents some localities of special interest to the student and col- lector of minerals. It is therefore of interest to embody in a special chapter the notes and experience gained while in the field. The minerals may be classed under three or four heads on the basis of association as follows, but it is not intended to include in the tist the ordinary rock-making minerals or others which do not exhibit some feature of special interest. The list amplifies in some respects the one given by the writer in the Geology of the Magne- ites near Port Henry, N..Y. (Am. Inst. Min. Eng: Vranas seg 27 :195 |. ? 1 Minerals of the Paleozoic limestones, embracing occasional calcite crystals and one occurrence of sulfur, derived from the alteration of pyrite. 2 Minerals of the Grenville limestones, and their associated in- clusions of silicates, viz: calcite, diopside, fluorite, garnet, graphite, . : 4 E | . | | | BLIZABETHTOWN AND PORT HENRY QUADRANGLES 153 hornblende, orthoclase, quartz of the rose variety, phlogopite, pla- gioclase, rutile, titanite, tourmaline, wernerite, wollastonite. 3 Minerals of the nontitaniferous iron mines. These are of two groups, according as they occur in the ore or in the associated pegmatites or pegmatitic segregations. In the ore proper, there is little beyond magnetite, apatite, calcite, hematite, molybdenite, and siderite, deserving comment and most of these are unusual. The interesting minerals are in the pegmatites and the list is quite large, albite, allanite, amphibole, apatite, arsenopyrite, , biotite, fluorite, garnet, lanthanite, magnetite, molybdenite, pyrite, pyroxene, quartz, titanite, wernerite, zircon. 4 Minerals of the titaniferous iron deposits, ilmenite, magnetite. The above species will now be taken up in alphabetical order with comments on the occurrence. Albite. In 1895 or 1896 the workings in the great pit of Mine “21,” encountered a large and coarsely crystalline pegmatite dike. Many carloads of this rock were brought to the surface,-of which a comparatively small part is still accessible in the easternmost dump along the main track toward Port Henry. From the peg- matite, cleavage masses of striated and slightly greenish feldspar ean sometimes be obtained. Cleavage flakes parallel with the base, give an extinction from parallelism to 3 degrees. On the brachy- pinacoid the extinction reaches 15 degrees. Prof. William Hallock determined the specific gravity of a piece weighing about 55 grams lo be 2.6182 at 14.5° C. This is slightly below the general aver- age (2.62) of albite, but undoubtedly the albite molecule predomi- uated in the piece. Still the general appearance, depending as it does on the greenish hue and the coarse striations, reminds one rather of oligoclase. Allanite. This mineral, usually esteemed a rare one, is present in unusual amount and has afforded some crystals of exceptional size and perfection. Allanite from this locality was first announced by W. P. Blake in the -American Journal of Science, September 1858, page 245. The occurrence was in the Sanford bed, or as “we now call it, the “ Old Bed,” the one just north of “21” and at present not much worked. Allanite crystals 8 or 10 inches long, 6 or 8 inches broad, and % inch thick are cited. The particular rock mass containing them was apparently long since exhausted, but one may still find small allanites in the pegmatitic streaks of this old pit. James Hall secured one of the large and very perfect ones in the early days and placed it in the hands of, E. S. Dana by whom it was described in the American Journal of Science for ThA NEW YORK STATE MUSEUM June, 1884, page 479. The spécimen was formerly in the Wale 2 collections and it certainly is an unusually fine crystal. a In later years the workings in the Smith mine, through the Cook — shaft have brought up much coarse pegmatite in which there are at times great quantities of large allanites, some of which almost ~ equal the dimensions given above. They are not always, or not very often well terminated, and being embedded in quartz and — feldspar, and being withal extremely brittle they require great care and patience for.their safe extraction. A series of the best secured by the writer were placed in the hands of Heinrich Ries in 1898, and were by him figured and described in the Transactions of the 4 New York Academy of Sciences, volume 16, pages 329-30, se =a The two figures, drawn by Dr Ries are here reproduced. . Figs. 31, 32 Allarite crystals from Cook shaft of Smith mine, Mineville (after Heinrich Ries) Amphibole. The most attractive member of this group is a light brown variety which is occasionally well developed in the quarries’ in the Grenville,north of Port Henry, The? crysraisep ~ to an inch in length by a half inch in the long diameter have grown from bunches of silicates into a cavity which has afterward been filled with calcite. When the latter is dissolved away, the former remains in almost perfect development. A sharp prism and both the orthopinacoid and clinopinacoid make up the vertical zone, and the terminal faces are a pair of pyramids. Dark green or black amphibole 1s common in the coarse pegma- titic aggregates associated with the magnetites on Barton hill. Where it abuts against quartz, it develops the face of the unit prism, but as a rule only cleavage pieces can be obtained. Apatite appears in great quantity in-the rich phosphorus ores — of the Old Bed series at Mineville. The grains may reach a quarter. of an inch in diameter and are usually of a red color from infiltrated hematite. They impart a red color to the ore itself and thus produce the variety known as red ore. This variety of apatite is separated in the mill and sold for fertilizer. . BLAZABETHTOWN AND PORT HENRY QUADRANGLES T55 In the pegmatitic aggregates from the Barton Hill mines, apatite appears in green hexagonal prisms, up to half an inch in diameter. It has also been noted as an inclusion in titanite, having’ preceded this mineral in time of formation. The angles of the crystals are more or less rounded as so often happens with this mineral. _Arsenopyrite is of rare occurrence in the coarse pegmatite of the “21” mine. It is associated with quartz, orthoclase, albite emcezircon, Although as a rule in thin seams long-cracks and cleavage planes, one specimen was found, about % inch long, by 1% inch broad and thick. It had, however, but one crystal face. Biotite occurs in the coarse pegmatitic aggregates of the iron mines, and in the bunches of silicates in the Grenville oe cuatries. It seldom exhibits crystal boundaries. Marette, Ihis taincral is of ‘course present in’ the Grenville limestone quarries and is occasional in the mines at Mineville. The most interesting occurrence is one discovered in 1888 by Mr W. H. Benedict, then principal of the Port Henry High School. ‘The crystals were measured and figured by the writer in a brief note in the American Journal of Science for July 1890, page 62, and the figure is reproduced in the 6th edition of Dana’s System of Mineralogy. Upon the faces of the unit rhombohedron, with sub- ordinate 4R, are superimposed two scalenohedrons whose combina- tion oscillating with R builds up a low, four-sided pyramidal form. The two scalenohedrons gave # R * and +? R 2 At Mineville the calcite appears in crusts consisting of well Ceveloped —4 R. The Miller pit has furnished the best spect- mens but they are not common. Diopside, see under Pyroxene. Feldspar. Albite has already been noted above. Oligoclase in great cleavage pieces has been collected from the old Cheever mine dumps and exhibits especially fine striations. Similar cleavage pieces may often be obtained from the pegmatitic masses of the cther mines. Labradorite is in endless quantity in the anorthosites. In the mountains along the Schroon valley it can be sometimes obtained in fairly good pieces, but as a rule throughout the area, the anorthosites have been so excessively granulated as to destroy the larger crystals. Orthoclase is common in the pegmatites but 1s seldom well crystallized. Yet in the area just south in Crown Point huge and well developed orthoclase crystals occur. Fluorite of massive character and not displaying other than cleavage faces ccurs in great abundance in the Barton Hill ore bed. The new tunnel which has been recently run from the Arch 156 NEW YORK STATE MUSEUM pit, so as to tap the lenses in depth, has cut large pockets of it, enough to form the entire wall on one side. The fluorite is white and has disseminated magnetite. It is near the lower workings of the Lovers pit. When this pit was in active operation it en- countered a peculiar, dense, green rock in small amount which, the microscope showed, consisted of quartz and actinolite. It con- tained scattered masses of fluorite of pink and green colors and up to 2 inches in diameter. : _ The most interesting fluorite of all, was however by chance obtained in one of the quarries in the Grenville limestone just north of Port Henry. A rather insignificant crust of dull yellow- ish color, proved to be this mineral, filled with the wormlike growths, technically called “helminths.” The commonest hel- minths are chlorite in quartz, but of what those in the fluorite consist 1s not known. Tig. 33 Helmiaths of some unknown mineral in fluorite. Actual fleld about .05 inch Garnet occurs in the North and South pits on Barton hill in excellent rhombic dodecahedra which are at times distorted so as to be greatly flattened. Aside from this occurrence well crystal- lized garnets have not been observed, but massive specimens of the mineral are not uncommon in both anorthosites and basic Heber aPOWN AND. PORT HENRY QUADRANGLES.. 7, syenites. In the sedimentary gneisses they also do not fail, and at times are very abundant. They are rich in the hill just east of Moriah Center and north of the Port Henry road and are of a pale pink. The commoner variety in the other rocks is deep red. Graphite is widespread in the Grenville limestones and in the thin associated quartzites, but does not seem abundant enough to imine in any observed locality. In the quarries north of Port Henry and in the coarsely crystalline calcite it sometimes exhibits sharp hexagonal crystals of diameters a quarter of an inch and less. In the pegmatite streaks it is coarser, but is seldom regular in outline. Hematite, pseudomorphic after magnetite occurs in the pegma- ererentie 21” mine. It is really martite, and retains the shape and cleavage of magnetite, while having a red streak. Some tabular masses of specular ore were met years ago at Fisher hill and were given the writer by E. B. Durham E. M., then engineer for the mining companies. Hornblende, see Amphibole. Fiypersthene, see Pyroxene. Ilmenite appears of massive character mingled with magnetite in the titaniferous ore bodies, but thus far no good crystals -have been discovered. These ore bodies are almost barren of good crystals. . Jasper has been afforded by a little vein in the Miller pit, Mine- ville. The quantity was small. Lanthanite was found in 1858 by W. P. Blake in association with the large allanites of the Sanford pit, Mineville, now called Cld Bed. It formed small crystalline plates and probably resulted from the alteration of the allanite [Am. Jour. Sci. Sept. 1858. p- 245]. Magnetite possesses especial interest not only from the great quantity which is available for mining but because in a large lense of ore developed in the early nineties in the Lovers pit slope of the Barton Hill mines, remarkably perfect crystals of this mineral ap- peared. The containing ore to the amount of 40,000 tons averaged over 68 per cent iron and carload lots ran 72. The crystals were buried in the granular ore and, as this crumbled readily, they were easily freed. While the greater number were more or less imper- fect from the interference of neighboring crystals or granules with their growth, there were found from time to time others up to an inch on the edge of the octahedron which were almost perfect. The faces of practically all the crystals are smooth and brilliant. The common forms were the octahedron with the rhombic: do“ec- & 158 NEW YORK STATE MUSEUM _ a ahedron modifying the edges. Locally and at the time of pro- duction for many miles. up and ca! the Delaware and Hudson — Railway the crystals were known as “diamonds.” During visieae to the mine the writer made a careful study of hundreds and endeavored to detect other faces, freely using the reflecting gonio- — meter in the measurements; but all the determinations led to such extraordinary indexes and to such variable results that the faces | were believed to be merely interference planes produced by con- ~ tact. The plane faces were found to be traversed by regular series of striations most of which follow the octahedral parting © planes, but others are parallel to still other faces as described ing the reference below to the writer’s paper on “ Gestreifte Magnetit- a krystalle.” | a The finest of all the crystals al magnetite from Minevitie is @ preserved in the office of Witherbee, Sherman & Co. at the mine @ and is about an inch in diameter. It is almost a mathematically — perfect octahedron, having only one slight interference plane on ~ one apex. Fortunately the matrix is also preserved but the crystal ~ is believed to have come from the Old Bed (or Sanford) pit. All the pits are from time to time sources of cleavage pieces — bounded by octahedral planes and often of large and regular size. a The apparent cleavage is, however, really due to a series of parting 4 Fig. 34. Magnetite crystal from the Split Rock mine ~ planes or gliding planes as is usually believed to be the case witha minerals of the spinel group. Rarely these plates exhibit brilliant luster. In the coarse pegmatite of the ” pit, moderately: large bat very fragile crystals of magnetite are not uncommon, which are dodecahedral forms built up of octahedral Sone planes, a very common feature of magnetite. Es 6¢ ry We bik. ‘ “; , a Pitz ben aTOWwWN AND PORT HENRY- QUADRANGLES 159 In the dump of the Split Rock titaniferous ore body the writer happened upon a few pieces, which had once formed the sides of a marrow crevice. They were coated with small but brilliant crys- tals which Mr H. P. Whitlock of the State Museum identified as magnetite of the form shown by the accompanying figure which he kindly drew. The crystals are remarkable for the development of the cube, a rare face in magnetite, and for the trigonal trisocta- hedron. The following papers have dealt with the magnetite crystals -from Mineville: Birkinbine, John. Crystaliine Magnetite in the Port Henry, N. Y. Mines. Pmeeee Vian, ne. Trans. 1800. 18:747. Kemp, J. F. Gestreifte Magnetitkrystalle aus Mineville, Lake Champ! ain Gebiet, Staat New York, Zeitschrift fur Krystallographie, 19:183. Notes Gmeoneevitdierals occurring near Port Henry, N. Y...Am. Jour. Sci. July, 1890, p. 62. Microcline, see under Feldspar. Moiybdenite, as is usual in the magnetic mines of the ancient gneisses, occasionally appears in the pegmatitic streaks. In the — New Bed pits it has been observed as scales associated with pyrrhotite. | Olivine is a common constituent of the gabbros but seldom if ever in amounts sufficient to see without the microscope. Phlogopite appears in the quarries in the Grenville limestones and ophicalcites, its characteristic association. Plagioclase, see under Feldspar. Pyrite is a rarity in the large mines and is only met in some secondary veinlets. It does appear in some of the smaller and leaner ore bodies but not, so far as known, in good crystals. Pyroxene being the name of a group, the several species under it must be taken up separately. Hypersthene, the orthorhombic member, is common in the anorthosites and gabbros, usually in the microscopic way; but when the former are coarsely crystalline and above all pegmatitic, the hypersthene assumes moderately coarse, platy growths which give cleavage pieces. Diopside appears in the quarries in the Grenville limestones. Once at the ophicalcite quarry a half mile north of Port Henry, the writer happened on pockets of calcite, into which diopside, brown hornblende and titanite projected in such a way as to be easily freed by weak acid. The diopsides vary from one tenth to half an inch in length and possess shining faces adapted to goniometrical measurement. They are usually white but shade to pink and are translucent. They have been measured and figured 160 NEW YORK STATE MUSEUM by Dr Henirich Ries in his valuable paper on the ‘ ‘ Pyroxenes of @ New York State,” Annals of the New York Academy of Sciences, - volume 9, page 171 and figures g and 10 on plate 14. They have yielded eight or ten of the faces found on the more com- plicated pyroxene crystals. Dr Ries analyzed the crystals with the results given under column 1 below. The specific gravity is 3.27, — : Much careful study has been given by Dr George P. Merrill to the diopside masses from which the serpentine of the ophicalcites q has been derived. An unaltered nucleus was separated by himemm and analyzed with the results in column 2. The. serpentine is — given in column 3. The two analyses of the diopside are strik- iiigly alike. : : 3 AEM © PD ai prema gree Pe Leni gr aes orl = BA ae 55:26 A2e 7 Cay n, Wateaanece Pe og carta geste Hele owe Poe aes BAAS i’ sae AN Most @ Par menses eines. crake tee rey Rh eat ct aie TF EZ S 19-53 Ale Lok) @ ererare gr San eMart e eo ed 1-80 57 64 SN Ig a Micaeine Pn as i wR Ey Peli Mere ig a aS: Bitte ty See eer | G1 © Bir dae eer ent fon ea hee aes Bc ue ar 270) Sas eo eee ASO Se Aes ane ee ee rege rie 22 30 TE CSO pote RE CA he Res ate el eye oe orn oat ss ee ene 22 1.57 Bemceh sees etches eaten 38. iso no Pa a O)ys eit ake cage Fe Sy ear ci cce cel ae hea oat eae ere 13n2 Total 0 oink ck keer an cere 99 .60 100.28 OO; 75 Each of these is almost pure diopside (CaMg)O. SiO,. Them serpentine evidently results from the disappearance of the lime _ and some of the silica, and the assumption of water. : In association with the iron ores and especially in the pegmatitic streaks involved in them crystals of black augite occasionally ap- pear. -One of these gathered by the writer at the Cheever mine has been figured by- Dr Ries in figure 8, pate 14 of his work just cited. An analysis yielded SiO» FeO CaO MgO AlLOs FeO: Total ail 49.12 15.98 17.30 6.06 7.49 3.58 99.48 4 Specific gravity 3.€0 s 2 “rom the presence of the sesqui-bases this is obviously an augite. In the ore of the Old Bed group at Mineville a pyroxene of an emerald-green color is frequent, and is similar to the one in the ncighboring syenitic rocks. Its color strongly suggests that it is related to aegirite and that it contains the soda-iron molecule in large amount. Pyrrhotite is rare in the larger mines although seen in some of the smaller sulfurous ones. It is not uncommon in the bunches BEIZASETHTOWN AND PORT HENRY -QUADRANGLES 101 of silicates in the Grenville limestone quarries and occasionally yields platy crystals suggestive of its characteristic forms but too rounded for sharp determination. Quartz. The large mines have yielded a few good quartz crys- - tals of the smoky variety. The pegmatites have corroded and rounded dihexahedrons. The most interesting occurrence is, how- ever, the rose quartz which is obtained in pits just west of the road from Port Henry to Cheever and about a mile and a half ftom the former. The color is very beautiful and the amount quite unusual. It forms veins in the Grenville series. Rutile appears in the bunches of silicates in the quarries of Grenville limestone, in somewhat scarce striated prisms and in irregular fragments. Scapolite, sce under Wernerite. Serpentine appears in masses often of very attractive ne green color in the ophicalcite exposures. An analysis is given above under pyroxene. . Siderite appears in small cross veinlets in the Miller pit. It forms a crust under calcite. Titanite appears both in the hornblendic masses in the Barton Hill ores and in the bunches of silicates in the Grenville limestone @uatries, especially the one just north of Port Henry. On Barton ailetney are of large size and beauty reaching 2 inches across. The faces are the usual combination of a steep pyramid and the prism. Wernerite has been yielded by the upper pits on Barton hill, in very excellent square prisms capped by the low pyramid. Fig. 35 Zircon crystal from Bie 36 Zircon crystal from Mire “21 Barton Hill mines Wollastonite occasionally appears in the Grenville limestones north of Elizabethtown. Its best locality is, however, in the Ausable quadrangle next north. | 162 NEW YORK STATE MUSEUM i Zircon occurs in the coarse pegmatite sent up in large quantities — from the “21” workings about 13 years ago, and now only avail- able in a few large lumps on one of the dumps. The crystals are ~% of great perfection although of simple forms. 110, 331 and_ 10. make up the combination. When fresh they are a dark mahogany brown, but some sort of alteration has changed the outer portions © of many crystals to an earthy, green and very tender material. The crystals vary in size up to an inch long and three eighths thick. Around them in the matrix are the usual radiating strain cracks. In the hornblendic. masses from the dumps on Barton = hill, one may rarely obtain small but brilliant zireons consisting of the prisms of the two orders, capped by the zirconoid and the unit pyramid. Figures of each of these are given on page 161 3 which were kindly drawn by Prof. C. H. Smyth. BIBLIOGRAPHY The following list of papers relates especially to the area covered by the bulletin. A short bibliography of the eastern Adirondacks will be found in Kemp’s Preliminary Report on Essex County, cited below, and in Van Hise’s Bulletin 86, also cited below. A review of the literature up to 1892 is given by the former in the Transactions of the New York Academy of Sciences, volume 12, page 19, 1892. Anon. Vacation Notes from Northern New York: On’ Post Wena Eng. and Min. Jour. Aug. 31, 1889. p. 1&6. | —— The Mineville Magnetic Mines. The Iron Age, Dec. 17, 1903. —— Port Henry Mines and Furnaces. The American Railroad Journal, 1840. Beck, L. C. Report on the Mineralogy of New Oe State. Albany 1842. p. r4-16. : Gives some details of the Cheever and Sanford Mines. Bell, Sir Lowthian. Notes of a visit to Coal and Iron Mines and Iron- works in the United States, . Read before British Iron and Steel Institute, 1875. Separate reprint, p. 21t. Describés his visit to Mineville. Compare also “‘ The Iron and Steel Institute in America,” Special Volume of Proceedings, 1890, p. 76. Birkinbine, John. Crystalline Magnetite in the Port Henry, N. Y. Mines. Am. Inst. Min. Eng. Trans. 1800. 18:747. ap Good account of the Lover’s pit, with notes, statistics and an lyses of tHe ores. F Blake, W. P.- Lanthanite and Allanite in Essex County, N.~ Y. Am. Jour. Sei Sept. 1858. p. 245. —— Mentions Blood Red Mica from Moriah. Jdem..-1851. p. ii, xi. Contribution to the Early History of the Mickastry: of Phosphate of Lime. in the, United: States) “Aim. “Inst... Min. ines dirans. 71892) eine Describes early attempts to utilize the apatite of the Sanford vein. —— Association of Apatite with Beds of Magnetite. Idem. 1892. a1 :159. Advocates stratified and organic origin of apatite and magnetite, ELIZABETHTOWN AND PORT HENRY QUADRANGLES 163 — Note on the Magnetic Separation of Iron Ore at the Sanford Ore Bear Vetian, Mssex ‘Co, N. Y., in 1852. Am. Inst. Min. Eng. Trans. 1892. 21 :378. : Brainerd, E. & Seely, H. M. The Chazy of Lake Champlain, N. Y. Am. Mus. Nat. Hist. Bul. 1896. 8:305-15. Brigham, A. P. Note on Trellised Drainage in the Adirondacks. Am. Geol. 1808. 21 :219-22. Clarke, J. M. Lake Champlain (abstract). Science. Sept. 27, 1907. p. 400. Cummings, W. L. On Sedimentary Magnetites. Engineering and Min- ing Jour. July 7, 1906. p. 25. Cushing, H. P. On the Existence of pre-Cambrian and post-Ordovician Trap Dikes in the Adirondacks. N. Y. Acad. Sci. Trans. 1896, 15 :248-52. —— Asymmetric Differentiation in a Bathylith of Adirondack Syenite. PomeeGeol, Soc. Bul, 19007. 18:477-92. Denaeehe es. On a Crystal of Allanite from Port Henry, N. Y. Am. Jour. Sci. June 1884. p. 479. Emmons, Ebenezer. Report on the Second District of New York. Albany 1842. Gives many geological details and notes on the mines, especially p. 236, 237. Granpery, J. Hi Phe Port Henry Iron Mines. Eng. and Min. Jour. 81 :890-93, 986-89, 1035-38, 1082-84, 1130-32, 1178, 1179. 1906. Hall, C. E. Laurentian Iron-ore Deposits in Northern New York, eer otare Wiis: Nat. Hist. 32d An. Rep’t. 1870. p. 133. Gives a general sketch of Adirondack geology and some details of the local mines. Hoefer, Hans. Die Kohlen- und Eisenerz-Lagerstatten Nord-Amerikas. aemia toys. p. 175-790. pl. 4, fig.. 14, 15. Gives an account of his visit and a plan and a cross section of the ore. Regards the Mine- ville group as a faulted series from same original. Hunt, TS: Mineralogy of the Laurentian Limestones. N. Y. State NMiseNat. Elist. 21st An. Rep’t. 1871. Geology of Port Henry. Canadian Naturalist. 2d ser. 10:420. Describes the local limestones as huge veins. The Iron-ores of the United States. Am. Inst. Min. Eng, Trans. Is00:. “£O:3. Refers to Lake Champlain mines. Kalm, Peter. Travels in America. English translation in Pinkerton’s Voyages and Travels, 13:374. Pages 604-15 speci- ally relate to Crown Point. Kemp, J. F. Notes on the Minerals Occurring near Port Henry, N. Y. Am. Jour. Sci. July. 1890. p. 62. Gestreifte Magnetitkrystalle aus Mineville, Lake Champlain Gebiet, Staat New York. Zeitschrift fiir Krystallographie. 19:183. — Geology of Moriah and Westport Townships, Essex County, N. Y., with a geological map, a map of the mines, four plates, four figures. N.Y. State Mus. Bul. 14. Sept. 1895. p. 325-55. Tescribes the local geology and mines. 164 . . NEW YORK STATE MUSEUM Preliminary Report on the Geology of Essex County. N. Y: Statem Geol. Rep i for 7o03) a psi4ee2: Does not touch specially on Moriah township, but gives a review and bibliography of the geology of the eastern Adirondacks. Gabbros on the Western Shore of Lake Champlain. Am. Geol. Soc: ‘Bale 1e0e mr Seana" . Refers to local gabbros. Crystalline Limestones, Ophicalcites and Associated Schists of the Eastern Adirondacks. Idem. 1894. 6,:24I. Gives details of local geology. ; Physiography of the Eastern Adirondacks in the Cambrian and Ordovician Periods. Am. Geol. Soc. Bul. 1897. 8:408-12. — Geology of the Magnetites near Port Henry, N. Y. especially those of Mineville. Am. Inst. Min. Eng. Trans. 1898. 27:146-203. ——The Titaniferous Iron Ores of the Adirondacks. U. S. Geol. Sur. igth’ An. Rept. 1e99.) (Pt 35" 2377-4122: —— The Physiography of the Adirondacks. Pop. Sci. Monthly, Mar. 19004 “ps 1Q5-210: See*comments by W. M. Davis, Science April 20, 1906, p. 630-31. The Mineville-Port Hénry Mine Group. N. Y. State Mus. Bul. r1o. 1908. p. 57-80. — & Marsters, V. F. Trap Dikes in the Lake Champlain Valley. U.S? Geol. SursBul® 107. Gives some details of locaktrap dikes. Lesley, J. P. The Iron Manufacturer’s Guide. New York. 1866. p. 388. Gives brief details of the mines. Maynard, G. W. The Iron Ores of Lake Champlain. British Iron and Steel Institute, 1874. -v. I. Merrill, G. P. On the Serpentinous Rock from Essex County, N. Y. USS o Nat. Mas. Proc 18008 -£2:505: Refers to local serpentinous marbles. Nason, F. L. Notes on Some of the Iron-bearing Rocks of the Adiron- dack Mountains. Am. Geol. 1893. 12:25. Newland, D. H. On the Associations and Origin of the Non-titan- iferous Magnetites in the Adirondack Region. Econ. Geol. 1907. 2 :763-73. | Geology of the Adirondack Magnetic Iron Ores. N. Y. State Mus. Bul. 119. 1908. Norton, S. New York Iron Ores. The Troy Times. March 12, Igo. Ogilvie, I. H. Glacial Phenomena in the Adirondacks and Champlain a Valley. Jour. Geol. 1902. 10:397-412. -—— Geology of the Paradox ass Quadrangle. N. Y. State Mus. Bul. 96. 1905. p. 461-508. Peet, C. E. Glacial and Post- place History of the Hudson ane Champlain Valleys. Jour. Geol. 1904. 12:415-69; 617-60. ; Putnam, B. T. Notes on the Iron Mines of New York. Tenth Census. 15:89. Contains excellent details of the mines. ELIZABETHTOWN AND PORT HENRY QUADRANGLES TOR. Pumpelly, R. Discusses shape of Miller Pit, from Putnam’s Notes... Tenth Census. 15:7. Raymona, P. BH. The Crown Point Section. Am. Pal. Bul. 14. 1902 p. 3-44. | faenee fauna of the Chazy Limestone. Am. Jour. Sci. - 1905. 20:353-82. Ries, Heinrich. A Pleistocene Lake. Bed at Elizabethtown, N. Y-. eeeoeevead. Sci. Frans, 1803. 13:197. — The Monoclinic Pyroxenes of New York State. N. Y. Acad. Sci. Ann. 9:124-80, and four plates. Gives many details of local mineralogy. Allanite Crystals from Mineville, Essex Co., N. Y. N. Y. Acad? Semetais. 1098. 16:327-20. Magnetite Deposits at Mineville, N. Y., etc. Mines and Minerals.. 1903. 24:49-5I. — Notes on Recent Mineral Developments at Mineville. N. Y. State. Mus. 56th An. Rep’t. 1904. p. r125-26. Smith, H. P. History of Essex County. Syracuse 1885. The data regarding the mines are chiefly taken from Watson’s?History, which see. Smock, if C. A Review of the Iron Mining Industry of New York for the Past Decade. Am. Inst. Min. Eng. Trans. 1889. 17:745. Statistical paper. See also Idem, 18: 748. Report on the Iron Mines of New York. N. Y. State Mus. Bul. 7. 1&8o. Taylor, F.B. Lake Adirondack. Am. Geol. 1897. 19:392-96. Van Hise, C. R. Correlation Bulletin on the Archean and Algonkian. U. S. Geol. Sur. Bul. 86. p. 308. Refers to local geology. van Ingen, G. & White, T.G. An Account of the Summer’s Work in Geology on Lake Champlain. N. Y. Acad. Sci. Trans. 1896. 15:19-23.. Watson, Winslow C. History of Essex County. Albany 1869. Gives a good historical sketch of the development of the mines. Woodworth, J.B. Ancient Water-Levels of the Champlain and Hudsor Valleys. N. Y. State Mus. Bul. 84. 1905. p. 265. - Wright, G. F. Glacial Observations in the Champlain-St Lawrence Valley. Am. Geol. 1898. 22:333, 334. a os Pe, 7 a ee INDEX Adams, M. K., analyses by, 46, 49. mulife, 20,. 41, 46, 50; 51, 54, 506, Ofent2s> Occttretice, 153. Allanite, 125, 126; occurrence, 153. Amphibole, occurrence, 154. Analyses, of anorthosite, 31-33, 36; dikes, 60-61; diopside, 160; gab- pags, AO: 55-56, 136, 139; iron Gres, 100, FOI, 104, 118, 119, 142, m43, 144, 145, 146; syenites, 45, 49. Andesine, 209. Mmeethite,.20, 34, 41, 43, 51, 36, 57, 62,53. Anorthosites, 27-44, 80, 81, 84, 94; analysis, 31-33, 30; border facies, 35; intermediate gabbros later than, 37; Split Rock Falls type, figures, 38, 39; distribution of, 85; Woolen Mill type, figure, 42; faulted, figure, 76; penetrated by gabbros, 126. Apatite, 35, 36, 40, 47, 48, 50, 56, Gris 6130, 134, 140, 145; occur- rence, 154. Archinacella? deformata, 7o. propria, 70. Areal distribution of formations, 79-88. Arsenopyrite, 125; occurrence, 155. Asaphus platycephalus, 74. Ashcraft brook, 18. Augen-gneiss, 28, 39. Wrueite, 25, 28, 41, 43, 48, 49, SI, fee 0G, 62, 123, 127, 120, 139, 142, 144. Bald knob, 13, 83. Barber point, 65. Barton brook, 62, 78. Barton gneiss, 124. Barton ills od, 1028 125. 20st, Barton hill group, 106, 116, 118-22, 123, 128, 120: . Basaltic dikes, 57-62; areal distri- bution, 8&8; faulted, figure, 77; figures, 58-59. Bathyurellus minor, 70. Bay State blast furnaces, 99. Beaver brook, 67, 68, 71. Beck) iC.) cited? 68, 1017162) Beede’s, 43. Beekmantown formation, 65-68, 75, 89, 90, 91, 94, 96, 150, I5I. Bell, Sir Lowthian, cited, 162. Bergschrunds, 17. Berkey, G—P., cited, 95. Bibliography, 162-65. Biotite 22). 2401205527... 30, 31, (40; AlpAgeA7, 51, 52, 54, 123, Tat, 1A2; occurrence, 155. Birdseye limestone, 72. Birkinbine, John, cited, 159, 162. Bisilicates, 56. Black river, 16, I4T. Black River group, 72-73, QI. Blake, WW. P. cited; 153, 162. Blueberry. shill 13. Blueberry mountain, 43, 87. Bonanza-Joker ore body, 106. Bond’s quarry, 64. Boquet river, 13, 14, 16, 18, 19, 20, 37, 54, 77, 86, 96, 135. Bostonite, 74, 94. Boulder clay, 93. Boulders, 94. ; Brainerd, E., cited, 65,67; 60, On, 163. Branch river, 13, 18, 20, 30, 50, 87. Brigham, A. P., cited, 16; 163. Brogger, W. C., mentioned, 32. Broughton ledge, 13, 14, 18. 168 Bucania sp., 69. bidorsata, 70. sulcatina, 70. Bulwagga bay, 67, 71, 73. Bulwagga mountain, 15, 26, 85, 92. Burt lot, 106, 120. Bytownite, 29, 34. Calcite, 37, 40, 50, 56, 140, 143, 145, 149; occurrence, 155. Calymmene senaria, 74. Camarella longirostris, 69, 70. varians, 69, 70, 7I. Camarotocchia, 71. Cascade, altitude, 12. Cassin formation, 68. Castaline, 135. Cedar point furnace, I50. Champlain, Lake, see Lake Cham- plain. Chazy, 75. Chazy 7 tonmatioin 1057.24 -Ol alow building and ornament, ISI. Cheever mine, 82, S3, 07,.08; 10355, 152. Chimney Point, 7, ot. Chlorine, 146. Chlorite, 47, 62. Chromite, 143, 144. Clarke, J M., cited; 163: lays) 63) 195)0152. Clionychia montrealensis, 7o. Cobble hill, 87. Cold Spring bay, 65, 68. Cole bay, 65, 68, 69, 74. Cole island, 65, 66. Columnaria alveolata, 73. fra nee. Cook. shait,; 120,126,140: Cornus ammonis, 8. Corundum, 140. Coughlin brook, 34, 86. Crag Harbor ore body, 100-3. Crais arbor, 67, 75) 625 63" (66; 146. Cross, Whitman, cited, 32. Crowfoot pond, 18, 27, 85, 86. Crown Point, 314,72; (Ol; 65 fois ecene of critical events in colo- mial history, 7; first use of name, “New York State MusEuM 7; taken by French, 7; captured by British, 8; fortification erect- ed, 8; plan of fortification, 8, 9. Crown Point peninsula, 68, 60, 72, 73, 88. Ctenodonta dubiaformis, 7o. peracuta, 70. Cummings, W. L., cited, 128, 163. Cushing, H. P., cited 25, 2702e 31, 35, 44, 64, 65, 68,°75, 81, Soy SOM 1245120, 103: Dana,- E. S., cited; 125) 54) e108? Deltas, 19-20. Derby, O. A., cited, 142. Dial, altitude, 12. Dikes, 14, 124, 125, 120; analyses: 60-61; basaltic unmetamor- phosed, 57-62, 88; figures, 58-59; trachyte, 74. Diopside, 20, 30, 33, 34, 355) 255s occurrence, 159; analysis, 160. Diplograptus, 74. Dix, altitude, 12. Drainage, 16-109. Durham, E. B., mentioned, 157. Eakle, A. S., analyses by, 60. Eccyliopterus fredericus, 70. proclivis, 70. Economic geology, 96-97. Egleston, T., cited, 99. Elizabethtown, 11, 84, I4I. Elizabethtown quadrangle, area, Io. Elm brook farm, 8o. Emmons, Ebenezer, cited, 22, 28, 75, 79; 93, 08; 100;2 ICO; aba Enstatite, 143. Eozoon canadense, 23. Eruptives, metamorphosed, 25-26. Escarpments, I4-15. Essex mining company, 98, 99. Eurychilina latimarginata, 60, 70. Faults, 75-70. Feeder pond, 146. Feldspar, 22,/27, 28, 30, 31, 345 0ag5 37, 38, 41, 43, 44, 45, 46, 48, 54, 60, 63; 124, 126, 127, 130; Ocelne rence, 155. INDEX 169 Ferro-vanadium, 148. Fisher hill, 106. Fisher hill mines, 120. Fletcherville, go. Fluorite, 125; occurrence, 155-56. Flux, 149-51. Fort Carillon, 8. - Fort St Frederick 8; plan of, to. Fulton, C. analyses by, 49. Gabbro dikes, faulted, figure, 77; intruded in -anorthosite and faulted, figure, 53. Gabbro-gneiss, 123. Gapbros, 31, 33, S81, 134; inter- mediate, later than the ariortho- sites, 37; Split Rock falls lo- cality, 37; Woolen Mill local- yoo, analyses, 40, 55-56, 136, 139; Woolen Mill type, fig- une, 42: New Pond locality, 43; basic. 52-57, areal distribution, S7e0in Cras Harbor ore body, 102; lying below Barton Hill ore body, 123, 124, 126; intrusive of larger masses, 1260; relations of to syenite series, 127; titanifer- ous magnetites in, 137. Seteter 22) 27, 31, 33, 35, 40, AI, Wapt472.54, 55, 50, 124, 126, 127, ient29, TAT. 142, 144, 145; oc- currence, 156-57. Gates mine, 133-34. Geikie, Sir Archibald, cited, 24. Giant mountain, 34; altitude, 12. Glacial and postglacial geology, 92-96. Glacial boulders, 94. Glacial scratches, 94. Gneisses, put with syenite series, 80; of Split Rock mountain, 84; -boulders, 94; in Crag Harbor ore body, 102; garnetiferous, 124; basic, lying below Barton Hill ore body, 124; assigned to syen- ite series in Barton hill_ map, 126; from Nichols pond, 133; in Gates mine, 134; in Nigger Hill mine, 135. Gothics, altitude, 12, Granberry, J. H., cited, 163. Gianites,) 26.27.0525 bution, 85. Grapiite, 22.0 26 157. Gravel, I51. Green: hillrsn. Green mountain, 12) 13) Grenville series) 21-25, 120, 127; faulted blocks of black horn- blende schist, in figure, 78; dis- tKibitionm, 82-65, at Port Henry, 89; limestone quarries, 96, 149; quarried and burned for lime, 150. Grove brook, 26, 82, 93. Gult, 15-16. areal distri- T45; Occurrence, Etat G i cited, ohO2: ally lames mentioned: «125. E53: Hall mine, 106, 120. Hallock, William, Ee Hammond brook, 62, 90. Harmony mines, 93, 106, 108, 116. Hargis aml ars So: Hawes, G..W., cited, 30. Maystack altitude, 12. Hebertella vulgaris, 60. Hematite, 97, 149; 157. Hillebrand, W. F., analyses by, 37, 40, 46, 55, 139, 142, 143, 144, 145, 146. Eitcheocl,,.G. El... cited, or: Hoefer, Hans, cited, 163. Hoisington brook, 16. Holiday pond, 20. Hormoceras tenuifilum, 72, 73. Hornblende; 22525; 27, 35, 40, 43; A4, 47, 48, 51, 52, 54, 101, 123, ¥24, E25. oe ToGeEAl, (LAD, E44, sass 157. Hornblende-gneiss, 127. Hunt, Rogers, acknowledgments £0, 105. Hunts ©. -S., ctted, 28, 32, 163. Hurricane mountain, 13. Hypersthene, 28, 30, 34, 35, 4I;, 47, 54, IOI, 123, 127, 129, 139, 142, 145,, 157. analyses by, occurrence, 170 Iddings, J. P., cited, 32. Ilmenite, 56, 61, 138, 439, 140, 142, 143, 144, 145, 146, 148; occur- nenee;: 157 Iron industry, historical outline, 98-99. Iron mountain, 14, 148. Iron ores, 97-149; analyses, 100, LOK, LOA UO, Wh LO; AD idiomas 145, 146. See also Magnetite. Isotelus harrisi, 69, 70, 71. obtusus, 70. Jackson brook, 150. Jasper, ocenrrence 157 Joker mine, 116. Jouct, CA. analyses by, 27, 40. Kalm, Peter, notes on _ local geology, 8; cited, 163. Kaolin, 33, 37, 40, 43, 50, 56, 62, I40, 145. Keeseville, 64. Kemp,. JE.) analyses) bya stay: Citeds 1Si32s AO. 02) N07 a Cos 102) 150" 163 Kent mine, 144. Kingdom, 141. Kingdom Works, 148. Kolderupe CG.) Beicited. yo: Labradorite, 29, 31, 38, 30, 43, 54, SO;187, WA2) 155. Lake Champlain, surface lowest point within area, 11; depth, 12. Lanthanite, occurrence, 157. Marsennc. o-, cited: 1130: Ledge hill mines, 140-41. Lee mine, 97, 98, I00. Leeds, Ay OR: canalyses by, soo; cited -32s Le Fevre, S., acknowledgments to, 105; mentioned, 146. Leperditia canadensis, 60, 70. fabulites, 73. limatula, 69, 70, 71. Lesley; J. Ba cited’ 104-5 Limekiln mountain, 84. Limestone, 149-52. Lincolne pond; 416; 14160 TA7e AS: pit near, 144-45. New YorkK STATE MUSEUM Lingula sp., 60. brainerdi) Goj.7 1 Little pond;: 87, 143744. Loon Lake, 44. Lophospira sp. ind., 70. peranoulata, 70. Lossing;: Bs Ji, cited aie: Lowville limestone, 72. 148; pits mean; Macadam, 149-51. McComb, altitude, 12. McIntyre, altitude, 12. McKenzie brook, 63, 64, 90, 149. Maclureas, 7I. iMaclurites, 66. logani, 73. magnus, 8, 60, 70; 71. Magnetite, 28, 31,33, 37 400s. 47, 48, 50, 51, 52, 53; 545 055a5e" 60, 61, 62, 87, 122, 123) nance 133, 140, 142, 143, 144, 145, 146, 148; OCCUIKENCES, = 1575595 nontitaniferous: 99-137; geologi- cal. relations, 122.257 envio the ‘ore, : 126-32: titaniferous: 97, 137-49; commer- cial” value 147. Mangerite, 40. Marble, serpentinous, I51. Marcy, altitude, 12. Marsters, V.-F., cited): 74suice Matthew, W. 1; citeditoy Maynard, G. W., analyses by, 139, TAR, AZ CiLedss 1GAe Merrill, G. P., cited, 23.. 1Gejsnez Metamorphosed eruptives, 25-26. Miucrocline, 26, -27,.1235 050: Microperthite, 27, 46, 49, 51, 52, LOT, 123 Mill brook,” 16; 27. a6: Miller ore body, 106, I14. Mineralogy, 152-62. Mineville, 11, 70, 93, 96, 97, O83 103} 127, 1 30; 134). 1A eras Mineville group, 105-19. Molybdenite, occurrence, 159. Monotrypella sp., 70. Moraines, 93-94. Morehouse, Frank, cited, 135. INDEX iz Moriah, I1, 93, 141; titaniferous ores, 140. Monat Center, I1,. 82, 93. Moriah Corners, II, 150. Moriah marble, 23, I50, 151. Morley, E. W., analyses by, 32, 46, 60. Moss ponds, 16. Mt Tom, 146. Mullen bay, 60, 72, 73, 74. Mullen brook, 74, 88, 89, go. iMemnoe, EH. S., cited, 129. ° Bason, Fo 1G.; cited,- 105, 164. New Pond, 14, 43. New Pond type, tion, 87. New Russia, 11, 18, 35, 37, 86, 95, tea, 4360; small pits near, 135. Mewland, D: H., cited, 134, 135, 164. Nichols Pond magnetite, 132-33. femenoison, Ft. A., cited, 73. Wigger Hill mine, 134-35. Nippletop, altitude, 12. Wobie mine, 133-34, 135. Norite, 54. Norton, S., acknowledgments to, 105; cited, 164. areal distribu- Oak hill, 35, 136, 148. Oak hill pit, 145-46. enigic, f H., cited, 17, - 164. Old bed ore bodies, 106, 122, 125, 126, 128, 129; figures, 107, I09, Beenie 10S, 117, LIQ, 121, 123. Olieeciase, 20, 123, 125, 155. Olivine, 54, 60, 62, 138, 140, I4I, mae 143, 144, 145, 1460; occur- rence, 159. O'Neill shaft, 106, 120, 122. Ophicalcite, 23, I5o. Ophileta, 66. Orchard-gneiss, 123. Orthidium lamellosum, 609. Orthis costalis, 66. platys, 60. Orthoceras sp. ind., 70. rectiannulatum, 73. 18; +05, Orthoclasen 345134, 3° 39, 41, 40, CO} 051, 50,402060,) 101, 1235 124, 125, 140, 145, 146, 155. Paleocystites tenuiradiatus, 70. Paleozoic strata :02-74;—1aults an, 75; areal distribution, 88-92. Parastrophia hemiplicata, 73, 74. Pease quarries, 23, 150. Peet, CE. cited,.03, 96; 164. Pegmatite, 26, 28, 125-26, 149. Penfield pond, 82. Phlogopite, occurrence, 159. Phosphorus, percentages of ores Lid Ae Phylloporina incepta, 66. Physiography, 11-20. Phytopsis tubulosus, 72. Buliershite: 123,163. 0lO3: Pilfershire mines, 78, 105. BiESSO twelve.) CIteC i 32) Pitkin. Ded. 135: Plaesiomys platys, 60, 70, 7I. Eiacto clasen20) «27,25, 20,5 30, ous Baio S0s 30 41 43; 40; 525,53; BAP CO, SOM NOT, 105, 122-1235 130) TAG, E42) TAn, 245). TAG, 150: Pleasant valley, 14, Io, 144. Plectoceras sp. ind., 70. sp. (probably undatus), 73. Plectorthis plicatella, 73. Pliomerops canadensis, 70. Port thleninyeenle ah47O2; 02, 75,2" 88, 89, 99, I50. Port Henry quadrangle, area, 10. Porter, altitude, 12. Potashe 30, 5su52. Potsdam, 64. Potsdam quartzite, 94. Potsdam sandstone, 21, 62-65, 75, 89, 90, OI. Precambric formations, 21; faults it, 76: Ptychoparia minuta, 64. Pumpelly, R., cited, 165. Putnam, B. L.,. cited; 76; 100); 164: 134, 135, 164. Putnam mine, 134. Pyrite, occurrence, 1509. Pynoxene,: 22) 25.0030) st ise. sO wea, 172 New York State Museum AG; 747, AS; lin ORO sige, 139,. 140; 145, .140; 14035" ocenr- Fence; 150: Pyroxenic anorthosites, 31. Pyrrhotite;-22) fo; 5 4is 247-9150: 2.50: LAO; 144, 2145) 140; (occurrence. fOU.Olwe: Quartz, 22, 25, 26, 27, 30, 33; 34, 35; 30, 40, 41, 45, 46, 47; 48, 50, 51, 52) OB AON, | £22, Won. BIO Eo: 133; asa geological thermome- ter, 130) OGcUrKeNnce, LOL. : Quartzite, included in anorthosite, figure, 34. Rafinesquina alternata, 69, 70. champlainensis, 70, 71. incrassata, 609, 70, 71. Raphistoma lenticulare, 73. stamineum, 7I. striatum, 70. Raven hill 1353 Raymond,” P.-E acited: 1607. 70g;-70, 725) M3; LOS. Redfield, altitude, 12. Reed quarry, 152. Rhinidictya fenestrata, 7o. Ries, . Heinrich) cited, 10,7 126,154 160, 165; analysis by, 160. Roaring brook, 20, 54, 93, 135. Rocky Peak ridge, 12. Ross ore bed, 136, 145. ROSSiy 2a o) pele <4: Rutile, 35; occurrence, 161. Saddleback, altitude, 12. Sand, 95, ISI. Sand dunes, 20. Sanford pit, 106. Saussurite, 28. Sawteeth, altitude, 12. Scapolite, 22, 125,146, TOT. Schist, 140. Schroon river, 16, 18, 20, 62. Schroon valley, 96. Schuchert, Charles, cited, 73. Seely, UM eited 65,567.01 102. Serpentine, 23, 62, 149; occurrence, 161. Serpentinous marble, 151. Shelburne point, 94. Sherman mine, 106, 120. Siderite; Occurrence, Lor Silica, *35,_.50: Sillimanite, 25. Skylight, altitude, 12. Slide brook, 86. Smith; G.- P. “citedsemore Smith mine, 106, 120, 122; %124sr2G. Smock,, J. C., cited; 132. 9143neess 165. Smyth, C. H:; jr, cited, te) etenene figures drawn by, 162. Spinel, 20, 56; 140, 144; 145 Split Rock, 144, 147, a4e: Split Rock-talls, 17, 18.037 Split Rock falls type, areal dis- tribution, 86. bc Split Rock mine, 138-40. Split Rock mountain, 84. Split Rock point, 84. Spotted mountain, 13. Stacy brook, 66, 84, 94. Standish, 99. : Steele ore bed, 84, 98, 136-38; fig- ure, 137. Steiger, George, analyses by, 35, 37, 55, 145. Stevens brook, 34. Stevenson farm, 89. Stoltz, G. C., acknowledgments to, 105. Stream terraces, 20. ~ Stromatocerium, 73. rugosum, 73. Strophomena incurvata, 73. Structural geology, 75-79. Sulfur, percentages of ores in, 147. Syenites, 44-52, 81, 123, 124, 126, 129, 135; analyses, 45, 49; areal distribution, 87; relation of gab- bros to, 127. Taylor, F. B., cited, 19, 165. Peall-oye yw td, pettede eau Tefft shaft ore body, 128. Tetradium cellulosum, 72, 73. Thaleops arctura, 70,271: INDEX 173 Thompson shaft, 120. Ticonderoga, 44. Titaniferous magnetites, commercial value, 147. Titanite, 22, 37, 43, 47, 50, 51, 122; occurrence, I6I. Titanium, 136. Tourmalin, 22, Trachyte, 94. Trachyte dike, 74. \s Trap dikes, 14. Treadway quarry, ISI. Trenton limestone, 73-74, QI, I51. Trinucleus concentricus, 74. Tryan, John, mentioned, 141. aryvan, pit, 148. Tunnel mountain, 147, 148. Tunnel mountain mines, 141-43. 137-49; inch, E. O,, cited, 68, 72. mentioned, 66: Vanadium, 147. Wan ise, C. R., cited, 16s. van Ingen, G., cited, 64, 165. Verd-antique, 23, I51. Wadhams Mills, 11. Walker brook, 509. Washington, cited, 32. Watertown limestone, 72. Watson, W. C., cited, 10, 135, 144, es 165. Welch ore: body-F210; 112: Wernerite, occurrence, I61. Westcott quarry, 84. Weston bed, 137. Westport, II, 14, 27, 62, 64, 65, 66, 68, 71, 73, 74, 75, 84, 89, 90, 95, I5I. 3 White, I. G.) eiteds i105: Whiteface, altitude, 12. Whiteface type, 35. Wichmann, A., cited, 32. Willsboro quadrangle, 84. Waachell, Ni Be, cited, 73: Witherbee, II. Witherbee, Sherman & Co., 105, 120. Wollastonite, 84; occurrence, 161. Woods hill, 84, I50. Woodworth, J. B., cited, 93, 96, 165. Woolen Mill, 37, 309. Woolen Mill type, areal distribu- tion, 87. Wright, F. E., cited, 130; test of rocks associated with the mag- netites, I3I. Wright, G. F., cited, 165. Young bay, 65. Zin.) 26;. 27,047, 50, 53,52, 122) 123, 125; occurrence, 162. Zygospira acutirostris, 60. recurvirostris, 73. ~ sejsuerpenb Arua 130g pue uMOITIOqRZITF 9q} Jo sdeur o1d0[0e5 = Bec ‘sft NITION’ WoasSAW sojsuespenb voued-uinqny ayy Jo deur a180]099 | 2 oS Ler NILATIOG waasnan aes | . > Sa ae a aySuexpenb uapAeT 310g at} Jo dent as01080 | k | Sex NILETIAS WOaSAW a. eee ee _ = : as fi ° ) =e ie peg IC F 3 b aoe a : : F XS ee > = S ; ra eee ee =) 5 ae ~ x —a ~ r : x ‘ t 5 2 | e \ mn > fs + \ ~ ‘ . - y . a é 4 \ = = 2 5 ~ R 2 ~ to we ‘ = -~ es pay Ne i ry \ i = rin t 2 by EDUCATION DEPARTMENT FOUN MC KE UNIVERSITY OF THE STATE OF NEW YORK STATE MUSEUM BULLETIN 135 PORT LEYDEN QUADRANGLE (Boonwilla) (MOK eever) TOPOGMAPHY BY V GEOLOGICAL sURver tm COOPERATION WITH THE STATE OF NEW YORK Wwontsen Scule oxhoo x 4 o a 2 x SS — 1 2 o x 2 3 . 3 Fee ea Sr ce Contour interval 20 foot Datusn to mesn #0 tered Geology by W. J. Miller, 1908. LEGEND Sedimentary Rocks Modern valley alluy- Tinon towethier with much Glacial drift. Sands and gravels, most- ly delta deposits, and Vargely concealing boundaries, J) Oswego sandstone. Gray, fine al, thin-bedded sandstone, ) Lorraine shales and sandstones, Alternating thin beds of gray to black shales and gray, fine-grained sandstones. Su =| Utica black shale. Somewhut calcareous to- ward base. Trenton limestone. ‘Mostly impure and thin- bedded in lower portion, and crystalline and heayy-bedded. in upper portion. ‘Sbr Black river limestone, Pore, bluish-gray, mas- sive limestone with chert nodules and a Little Ie. Lowville lim Pure, bluish, doye-col- ored, thin to thick bedded limestones, con- taining calcite-Alled tubes. Pametia timestone. Im. ire, i | to thtitha iesag wba ars: ‘stones. Sandstone and conglomerate at the base, = Metamorphic Rocks. Syenite. A rather quartzose rock, show- ing « gneissic stracture, and of undoubted ig- neous origin. Youngur than the Grenyille. Granitiesyenite. A very quartzose phase of the normal syenite gneiss, ‘The rock is nsually red. straight-banded, and contains long, narrow amphibolite’ inclusions, Grex gneisses. Highly metamorphosed, sedimentary rocks, showing a distinct gneissic stracture. Syenite-Grenville mixed gneisses. Clearly gneis- void rocks of | yarn types, bt mostly Gren- ville, anol cut up. by Intrusions of syenits. Precambric mocks, but of unknown, character Heeause. buried under heavy Glacial drift. | Stone Quarries. AB, GD, and BF are structure section lines. See text page 3. PLEISTOCENE UPPER SILURIC LOWER SILURIC PRECAMBRIC 4 — 4N39015)31d SINOAIO “A a We rr NNW NN wune oP ONS OSS Brame oot) NS NEA \ tot | 0) \ Sa ge oe pe ANI oiwue oiwae sowrg C2 so\prwouwns onus oiwu aowla m i Sa = _ Foti “ q % | ia Ss As euossertt } } = - } \ — wpuoNO euowepuwe ONIIS ¥3ddN ounyTaea nas oy sm uiitwo. S3TONVYOYN® YON39-NunEny _ Wy 4e1 NiLaTINE maoA man Ad : -* ; = aoe ‘aaa : Agro 07080 | ae 8 AN3WLuyd30 NoLLVonaa SWviis si 40 ALISHAAINA —, Win; oa y “hi a Bs a aie inal af . LARKE sT : ATE MUSEUM BULLETIN 138 STATE GEOLOGIST A Ree Peay Weed FP OK Lp, Ae LS, oe eS! a oe cd = 7 a ia fe 4 Limestone Sea level iD Beekmantown Limestone Potsdam Sandstone Crystalline Schists and Igneous Rocks SECTIONS ALONG LINES INDICATED ON THE GEOLOGIC SHEET SMITHSONIAN INSTITUTION LIBRARIES “HOACMTATMO ATA 9088 01300 6150