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BRARI Es SMITHSONIAN _ INSTITU < = < a WS AZ 5 2 NS = E: SS by oO = 2 =: oO ’ \ XS * = (@) WS \ Y 2 g 2X 2 2 N& yy *= z= E WO 2 = = > = ye = w ; a w) ae rT; RIES SMITHSONIAN INSTITUTION NOILOLILSNI NVINOSHLIWS S31uV (7p) = wn z owe ” | dah ST 2 eee ee Ge OU ee ‘ a xz ae ft. * a; a. y we i ait | : J Ney Sean if i AAT hale f ae » a tp th ei ‘oan en be Ue ee mie WITH THE AUTHORS COMPLIMENTS. 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. 489 ALBANY, MEY: FEBRUARY 15, IQII New York State MUSCU Dh nn \{ Nn Joun M. CrarKe, Director Z NS gonlon NStit,, Museum Bulletin 146 fc. P a é ‘ GEOLOGY OF THE NEW YORK, CTX (CATSKILL) AQUEDUCT === STUDIES IN APPLIED GEOLOGY COVERING PROBLEMS ENCOUNTERED IN EXPLORATIONS ALONG THE LINE OF THE AQUEDUCT FROM THE CATSKILL MOUNTAINS TO NEW YORK CITY BY CHARLES P. BERKEY , | * PAGE | PAGE Introduction and acknowledg- Ciecorr he Rondout valley sec- PARTI 8 2s, AEN Braet 5 {EVO} CS ae ae) ee ae 125 Th allkill Valley sec- PAtceneral features... os. 065.00. 9 7 on Rea hate i: ie 2 wey 149 Ch. 1 Catskill water supply 8 Ancient Moodna Valley.. 153 PEOIEGi pee po ieee 9 9 Rock condition of Foundry 2 Problems encountered in TOM kee wat ias (he Moana 163 the rOgectseng yy Rouen 17 10 Geology of Sprout brook. 171 3 Relative values of differ- | II Structure of Peekskill ent sources of informa- Checkley yc. ae me 175 tion and stages of devel- 12 Croton lake crossing..... 183 GPM Ave katie ae oe 25 13 Geology of the Kensico 4 General geology of the Com See oh ge one IQI TOOUGI gio Py eho ks 29 14 Stone of the Kensico : GUIEERITCS RSNA a a Nae 195 II Geologic problems of the 15 The Bryn Mawr siphon.. 201 PREC MEE As aa ty hia 75 16 A study of shaft 13 and SUE O8 (S610 A pea On as A 75 vicinity on the New Cro- Ch. 1 General position of aque- ton aqueduct....... BAe oy CIC Soe oe Sip 17 Geological conditions 2 Hudson river canyon.... 81 affecting the location of 3 Geological conditions delivery conduits in New affecting the Hudson York city SS cbol ap areaecy ce coe PCLC 215 PIVET (CTOSSHIGs <4 Sere ee 97 18 Areal and _ structural 4 Geological features in- geology south of 59th volved in selection of site street. ........ 8 Hae nisl etpic 231 for the Ashokan dam.... 109 19 Special exploration zones. 237 5 Character and quality of 20 The general question of the bluestone for struc- postglacial faulting...... 271 Hird purposes....0. esas BUG Me Mere erate Lote ie Wak waco epdim: Ccs OF i | “a ALBAN Y¥. UNIVERSITY OF THE STATE OF NEW YORK IQiIl M232r-Apt1o-2500 } f % ; i tS p 4 Be : 1913 IQI7 1919 IQI4 Igi2 1918 1922 IQI5 IQII 1920 1916 IQ21 STATE OF NEW YORK EDUCATION DEPARTMENT Regents of the University With years when terms expire WHITELAW Rerp M.A. LL.D. D.C.L. Chancellor New York St CLrarrn McKetway M.A. LL.D.Vice Chancellor Brooklyn DanieL Beacu Ph.D. LL.D. - =— — — = Watkins Puiny T. Sexton LL.B. LL.D. — \-—- — — = Palmyrm T. Guitrorp Smith M.A. C.E.LL.D. - - - Buffalo WiiiiaM NottincHaM M.A. Ph.D. LL.D. - — Syracuse CHESTER S. Lorp M.A. LL.D. - - - — -— New York © ALBERT VANDER VEER M.D. M.A. Ph.D. LL.D. Albany EpwWARD LAUTERBACH M.A. LL.D. — -— — — New York EuceENE A. Puitpin LL.B. LL.D. -—- - - -— New York Lucian L. SHEDDEN LL.B. LL.D. - - - -— Plattsburg- Francis M. CARPENTER - —- -—- -— — -— -— Mount Kisco Commissioner of Education ANDREW S. DrapeErR LL.B. LL.D. Assistant Commissioners Avucustus S. Downinec M.A. Pd.D. LL.D. First Assistant CHARLES F. WHEELOCK B.S. LL.D. Second Assistant Tuomas E. Finecan 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, GEorGE M. Witrey M.A. Attendance, JAMES D. SULLIVAN Educational Extension, WILLIAM R. Eastman M.A M.LSS. Examinations, HARLAN H. HorRNER 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. ABRAMS Ph.B. S P New York State Education Department Science Division, April 6, 1910 Hon. Andrew S. Draper LL.D. Commissioner of Education str: The extraordinary engineering operations which have been undertaken in the effort to provide the city of New York with an adequate wat:r supply have illuminated in most unexpected manner the geological structure and history of the region of the Hudson valley south of the Catskill mountains. So broad has been the scientific scope of this engineering problem and so direct its de- pendence on geological structure that the Commissioners of the New York City Board of Water Supply early found it of essential moment to enlist in their service a corps of trained geologists. In 1909 an agreement was effected between the Board of Water Supply and the State Geologist, in pursuance of which the geolog- ical data acquired in the preliminary and final surveys for the aque-_ duct were intrusted to Dr Charles P. Berkey, a member of the staff of the board as well as of the geological survey, for summation and presentation of their broader and more important bearings. I transmit to you herewith Dr Berkey’s report thereupon, entitled Geology of the New York City (Catskill) Aqueduct. It is a document of high value not only in enlarging and perfecting our knowledge of the geological structure of the commercial center of the United States, but its data and conclusions must prove of pro- found importance to all large engineering and architectural propo- sitions concerned with the region of the lower Hudson valley. [3] 4 NEW YORK STATE MUSEUM I therefore submit this, subject to your approval, for immediate publication as a bulletin of the State Museum. Very respectfully JoHN M. CLARKE Director State of New York Education Department COMMISSIONER'S ROOM Approved for publication this 7th day of April 1910 BIO Commissioner of Education — a <2 SEATENST: ATLANTIC . OCEAN copyrighted ISN? by Brvedwey Mezstine The Catskill and Croton water supply systems of New York city 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. 489 ALBANY, N.Y... FEBRUARY I5, IQII New York State Museum Joun M. Crarke, Director Museum Bulletin 146 GEOLOGY OF THE NEW YORK CITY (CATSKILL) AQUEDUCT STUDIES IN APPLIED GEOLOGY COVERING PROBLEMS ENCOUNTERED IN EXPLORATIONS ALONG THE LINE OF THE AQUEDUCT FROM THE CATSKILL MOUNTAINS TO NEW YORK CITY : BY CE AKUES P BERKEY EV EFRODUC TION AND ACKNOWLEDGMENT It is the writer’s hope that the series of studies brought together in this bulletin may help to effect a wider appreciation of the prac- tical usefulness of geology. The volume contains a summary of the local geologic facts and the general principles found helpful in solving some of the problems encountered in a single great engineer- ing enterprise. The summary is accompanied by brief discussions of the methods employed and of the final results or conclusions reached. It is therefore essentially a study in applied geology. Seldom has so favorable an opportunity been afforded to follow extensive exploratory work and check geologic hypothesis or theory by subsequent proof. And still more seldom have engineers in charge of similar works so fully appreciated the value of geologic investigations and the extent to which they can be utilized as a guide. More credit is due to Mr J. Waldo Smith, chief engineer of the Board of Water Supply of the City of New York, than to any one else for appreciating the importance of the geologic complexity of [5] 6 NEW YORK STATE MUSEUM the Catskill Aqueduct problem. His exceptional insight into- its nature led to the adoption of measures in this direction that are now proved to have been fully justified. A staff of geologists has been maintained. From time to time engineers of the regular staff who have shown unusual aptitude in such investigations have been assigned to special duty on geologic exploratory work. In the pre- liminary investigations of the Northern Aqueduct, Division Engineer James F. Sanborn was very intimately connected with the geologic work. With him the writer worked out many field studies that later formed the basis of advisory reports, covering locations, kinds of explorations to be made, and interpretations of data. No one has had a better grasp of both the geologic and the engineering aspects than Mr Sanborn. It is with great pleasure that the writer acknowledges many valuable suggestions and much help through association with him. In the later exploratory work within the city similar service has been rendered by Mr John R. Healey, who has much to do with the geologic detail-of the delivery conduit data. The consulting geologists employed by the board were Professors James F. Kemp, W. O. Crosby and the writer. A special debt is acknowledged to Prof. James F. Kemp, consult- ing geologist of the board, whose confidence in the writer’s work originally brought him into touch with these investigations as an assistant, and with whom since that time many joint reports to the board have been written. Valuable advice and assistance in arranging for the issue of this report has been given by Department Engineer Alfred D. Flinn of Headquarters Department. For some of the corrections and sug- gestions special ackiowledgment is made to Department Engineer Thaddeus Merrimar , The department engineers, Robert Ridgway of the Northern Aqueduct, Cariton E. Davis of the Reservoir, Merritt H. Smith, for- merly of the Southern Aqueduct, Frank E. Winsor of the Southern Aqueduct, William W. Brush and Walter E. Spear of the City De- livery have given every facility for gathering geologic data within their territory and have contributed largely to the better understand- ing of their special fields. The geologic matter relating to special problems has been. worked out with the aid of the division engineers in direct charge in the field. Among these must be mentioned L. White of the Esopus division, William E. Swift of the Hudson river division, A. A. Sproul of the Peekskill division, Lawrence C. Brink of the Wall- GEOLOGY OF THE NEW YORK CITY AQUEDUCT i kill division, J. S. Langthorn of the Ashokan reservoir, Wilson Fitch Smith of the Kensico division, T. C. Atwood of the New York city delivery division. The data included in the tabulation of this bulletin have been gathered largely by others. Many of the explanations and conclu- sions are the outgrowth of the work of engineer and geologist, together. A large number of associates are engaged on this public work in such relations to one another that the individuality of each is obscured in the common effort to reach an enviable efficiency and success for the whole enterprise. The combined efforts of many, unselfishly given, have thus brought together a total far in excess of what any one individual could accomplish. Acknowledgments should therefore be made to those members of the staff of the Board of Water Supply who can not in the nature of the case be mentioned by name. Were it not for their cooperation the great mass of data here summarized could not have been compiled. CHARLES P. BERKEY Special Geologist, New York State Geological Survey; Consulting Geologist New York City Board of Water Supply Columbia University, New York City November 1, 1910 I GENERAL FEATURES CHAPTER f CATSKILL WATER SUPPLY PROJECT New York city obtains its chief water supply from the Croton river watershed. Other sources! now drawn upon are less important although some of them, such as the Long Island underground supply, are capable of considerable additional development. The average daily consumption of Croton water was approximately 324,000,000" gallons for 1907. At the present rate of increase of population the consequent daily increase in consumption of water is 15,000,000 gallons in each succeeding year. The entire daily flow of water in the Croton river for the 18 years from 1879 to 1897 averaged only 348,000,000 gallons. About 10,000,000 gallons per day is lost by evaporation and seepage from existing reservoirs. The records for 40 years, from 1868 to 1907 make a somewhat better showing. Making no allowance for evaporation the average flow amounts to 402,000,000 gallons. With due allowance for evaporation,? however, this only increases the daily supply as now planned by about 47,000,000 gallons. That is, the possible total additional water within the Croton watershed would suffice for only three years’ growth of the city. Much of this additional water belongs to periods of excessive precipitation. To save it would require additional storage facilities for 305,000,- 000,000 gallons, and, it is estimated, would probably cost $150,- 000,000. 1 Brooklyn is in part supplied by these additional sources which furnished 145,000,000 gallons daily in 1907. 2The figures used here as to consumption and capacity and available supply are taken from the printed statements of the commissioners of the New York City Board of Water Supply in a circular dated April 16, 1908, and are based upon the investigation and reports of the corps of engineers headed by J. Waldo Smith, chief engineer, John R. Freeman and William H. Burr, consulting engineers. The reports of this commission and various others that have had the responsibility of investigating the future supplies for New York city have been drawn upon freely for such data. 3 The average rainfall for the past 40 years is about 49 inches per year. Only about 48 per cent of this runs into the streams. The rest evap- orates or is absorbed by the vegetation or joins underground supplies that do not again appear at the surface in the district. [9] IO NEW YORK STATE MUSEUM Taking into account the small relief possible in this direction and the certainty that in less than five years the demands of the city will be greater than the total capacity of the Croton watershed, it is clear that some other source of large and permanent supply is an absolute necessity. | In the search for such additional sources, there has been much careful work done by able commissioners.t. In the meantime, resi- dents of certain districts where there are possible supplies have taken steps by legislative action to effectually? prevent New York city encroaching upon their territory. Criticisms? of all kinds largely by those only partially informed as to the magnitude and complexity of the problem and partly by those ignorant of the simplest factors in its solution, have been kept perpetually before the public. One needs only a slight acquaintance with such public works to realize that it is much easier and more common to criticize and raise the cry of corruption or incompetence than it is to give really valuable advice or solve a real problem or carry an enterprise of the most vital public importance to a successful issue. It is sufficient here to observe that exhaustive studies of the whole question of water supply by competent men have resulted in a practically unanimous conclusion that the streams of the Catskill mountains are the most satisfactory, economical, reliable, abundant and available future source of water. 1 The Report of John R. Freeman C. E., 1899-1900; Report of the Burr- Herring-Freeman Commission, 1902-4; the Studies of the Department of Water Supply, Gas and Electricity, 1902-4; Investigations of the Board of Water Supply, 1905 to the present time. 2 Acts of the Legislature of 1903-4. 3 The commonest suggestions neglect the question of permanence or constancy of supply. The following sources are often mentioned, (a) Lake George, forgetting that this beautiful lake has an abnormally small water- shed and could never figure as a large permanent supply; (Db) artesian wells, ignoring the fact that with the exception of certain portions of Long Island there is almost no artesian capacity, and on Manhattan and the mainland the crystalline rocks make such development useless; (c) Lake Ontario, apparently overlooking the great distance (400 miles) and the many other complications that this international water body involves; (d) the Housatonic river, neglecting the difficulties of interstate origin; (e) Dutchess county, where the city is prohibited by legislative enactment; (f) the Hudson river, ignoring the fact that the Hudson is an estuary of the sea with brackish water of a very impure quality and wholly unfit for domestic uses. It is, however, worth while to note that Hudson river water is sure to be used more and more extensively for fire protection and similar purposes in the more densely populated portions of the city by means of an entirely different system of conduits. This is one of the most promising directions of relief looking to the more distant future. GEOLOGY OF THE NEW YORK CITY AQUEDUCT ‘ee XTE ——— The Catskill supply will furnish over 500,000,000 gallons of water daily and was estimated to cost $161,857,000. That is, the additional supplies from the Catskills as planned will, when com- pleted, be sufficient for the increasing demands_of the growing city, for the next 35 years. And some of it may be badly needed long before it can possibly be delivered. Parts of the Catskill system? The chief sources within the Catskills now included in the plans - of the board are: I Esopus creek, to be taken at a point near Olive Bridge. 2 Rondout creek, to be taken at a point near Napanoch. 3 Three small streams tributary to the Rondout. 4 Schoharie creek, to be taken at a point near Prattsville. 5 Catskill creek, to be taken at a point about 1 mile northeast of Durham. 6 Six small streams tributary to the aqueduct between Catskill creek and Ashokan reservoir. The comparative areas of watershed and their daily capacity are estimated? by the corps of engineers as follows: _ | AREA | | ages STORAGE IN DAILY SUPPLY MILES GALLONS IN GALLONS came | | fe SOEs WeaketShed 0. 56/0'.:...:. ue 70 000 000 0008! 250 000 000 2 Rondout watershed....-...| 131 20 000 000 000 | 98 000 ooo 3 Three small tributaries...... | Paap pase Sota Ws eee Eee he | 27 000 000 4 Schoharie watershed........ | 228 45 ©00 000 000 | 136 000 ooo 5 Catskill watershed......... 163 30 000 000 000 | I00 000 000 Goat, stanlbetreams. 020%...) Oe ey eae ee Ge a 49 000 000 C170 [£2 sh ea Been a irae 904 165 000 000 000 | 660 oa0 000 1 The subdivisions and proposed locations given here are taken chiefly from the Report of the Board of Water Supply of the City of New York to the Board of Estimate and Apportionment, October 9, 1905. 2 Estimates are much more complete for the Esopus, which it is planned to develop first, than for any other streams; and it must be understood that the figures are subject to revision dependent upon modifications of original plans to meet the conditions that develop upon more elaborate investigation. 3 Preparations are to be made for storage of 120,000,000,000 gallons of water on the Esopus, but a part of this capacity is intended to accommodate supplies drawn from other sources than Esopus creek itself. LONGSNOV GNV SGSHSYSLVM TIUASLVO Or j ATA BN 92 Gul Avg 10389 Bay nay Y ASIOALIS9, ! fe MIA IH 4 = o ~ ajedaayySnog GEOLOGY OF THE NEW YORK CITY AQUEDUCT I3 The evident certainty that present supplies from the Croton and Long Island will be very inadequate long before the Catskill system can be completed has influenced the adoption of plans contemplating the construction of certain parts in advance of the rest. To begin with, only the Esopus watershed is to be developed by the con- struction of the great Ashokan dam at Olive Bridge making the reservoir of full capacity. At the same time that portion of the aqueduct between the Ashokan dam and the present Croton reser- voir is to be completed in advance of other parts so as to make it possible to turn additional supplies into the Croton system, the capacity of the present Croton aqueducts being somewhat in excess of the Croton storage in dry years. It is furthermore desirable that increased storage capacity should be secured much nearer to New York city, and with that end in view Kensico reservoir is to be greatly enlarged. It is estimated that this may be made to hold 50 days’ supply of 500,000,000 gallons daily. The development of the Catskill system is being carried on by the Board of Water Supply, which was appointed by Mayor McClellan, as provided in chapter 724, of the laws of 1905. The present board consists of John A. Bensel, president, Charles N. Chadwick and Charles A. Shaw. The Engineering Bureau of the Board is in charge of J. Waldo Smith, as chief engineer, Merritt H. Smith, as deputy chief engineer and Thaddeus Merriman, assistant to chief engineer. Influenced doubtless in large part by the unity of certain portions of the project, either because their essential engineering features are distinct, or because their construction is more urgent, or in order to facilitate the work of supervision of so great an undertaking, the following departments have been created: 1 Headquarters department (executive). In charge of general designs, plans of construction and preparation of contracts. Alfred D. Flinn, department engineer. 2 Reservoir department. In charge of development of the Cats- kill watershed and the construction of the various dams and res- ervoirs. Carlton E. Davis, department engineer. 3 Northern aqueduct department. In charge of the construction of full capacity aqueduct from the Ashokan dam (60 miles) to Hunt- ers brook in the Croton system. Robert Ridgway, department engi- neer. 4 Southern aqueduct department. In charge of the construction of full capacity aqueduct from Hunters brook in the Croton system I4 NEW YORK STATE MUSEUM to Hill View reservoir on the northern limits of New York city and of the storage reservoirs and filtration work. Merritt H. Smith, and more recently F. E. Winsor, department engineer. 5 Long Island department. In charge of the development of the underground water supply of Long Island. A plan looking toward ~ this end has been prepared and approved by the city authorities and is now being reviewed by the State Water Supply Commission. 6 City aqueduct division. In charge of the delivery of water from Hill View reservoir throughout Greater New York. Origi- nally in charge of W. W. Brush, now under Walter E. Spear, as department engineer. Departments are further divided into “ divisions” each in charge of a division engineer and a full corps of assistants. The subdi- visions of these larger units, although primarily based upon con- venience and efficiency of engineering supervision, coincides rather closely with the larger geologic problems included in this bulletin. ' Generalities of construction The chief types of structure projected include (1) masonry dams, (2) earth dikes with core walls, (3) “cut and cover” aqueduct through country of about the elevation of hydraulic grade, (4) tunnels through mountains or ridges that are too high, and (5) pressure tunnels under valleys or gorges that are too low. Some of these are oi record proportions. For some of the de- tails and figures see the different special problems in part 2. All items complete as planned involve a total of: Io dams IO impounding, storage and distributing reservoirs 4.5 miles of dikes 54-5 miles of “cut and cover” aqueduct 13.9 miles of tunnel at grade 17.3 miles of pressure tunnel below grade 34 shafts of aggregate depth of 14,723 feet. 6.3 miles of steel pipes making 92.5 miles of aqueduct compiete to Hill View equalizing reservoir 1 filtration works 18.0 miles of delivery tunnel in New York city to the termina! shafts in Brooklyn 16.3 miles of delivery pipe lines GEOLOGY OF THE NEW YORK CITY AQUEDUCT 15 Allowing for contingencies and costs for engineering supervision the system is estimated to cost $176,000,000 and many years will be required for its completion. The present plans, however, con- template only the immediate development of the Esopus watershed. the storage reservoirs near the city and the main aqueduct to the various points of delivery within the city limits. It is expected that part of this additional supply of water will be available by the year 1913, or early in 1914. GHAPTER IT PROBLEMS ENCOUNTERED IN THE PROJECT When the Ashokan reservoir is filled the surface of the stored waters will stand 590 feet above the sea. Hill View reservoir on the northern borders of New York city will have an elevation of 295 feet. The distance between these two points is nearly 75 miles in direct line. The contour of the country and other exigencies of construction will increase this to approximately 92 miles. A main distributary conduit in New York city will add 18 miles more. The destination of the water therefore before distribution begins is 300 feet lower than its starting point. This is sufficient head to permit gravitational flow and a self-delivering system. If the hy- draulic gradient can be maintained it would evidently constitute a decided advantage. The plans have therefore from the beginning contemplated such construction. It means then that a flowing grade must be maintained in all tunnels or channels or tubes and that when a depression has to be crossed the pressure must be maintained in some sort of a conduit so that the water may rise again to a suitable level on the other side. The difficulties of accomplishing this in a work of such magnitude are not at first apparent. The full significance of the undertaking can be realized only after a study of the country through which the aqueduct must be carried. It then resolves itself into a series of problems, each one having its own characteristics and peculiar difficulties and methods of solution and each requiring a thorough understanding of the topographic features of the vicinity and a working knowledge of geologic conditions. 3 General questions It is sufficient at this point to call attention to the facts of the topographic map and point out only the most general physiographic features that may at once be seen to materially modify the simplicity of the line. For example, one has scarcely left the great reservoir, with water flowing at 580-90 feet above tide, before the broad Rondout valley is reached, with a width of 4% miles nowhere at great enough elevation to carry the aqueduct at grade. If it is to be crossed at all, and it must be crossed to reach New York city, some [17] 18 NEW YORK STATE MUSEUM special means must be devised. If a trestle be proposed, one finds that it would have to be 4%4 miles long (24,000 feet), and in some places 300 feet high, and at all points large enough and strong enough to carry a stream of water capable of delivering 500,000,000 gallons daily —a stream that if confined in a tube of cylindrical form would have a diameter of about 15 feet. : A steel tube might be laid to carry the water across and deliver it again at flowing grade, but here one is met with the fact that it would require a tube of unprecedented size and strength and if divided into a number of smaller ones the cost would be greater than that of a tunnel in solid rock. The other alternative is to make a tunnel deep enough in bed rock to lie beneath surface weaknesses and superficial gorges and in it carry the water under pressure to the opposite side of the valley. This is the plan that seems best suited to the magnitude of the undertaking and would seem to promise most permanent con- struction. But no sooner is this conclusion reached than it is realized that there are now several hitherto unregarded features’ that assume immediate and controlling importance. Some of these, for example, are (1) the possibility of old stream gorges that are buried beneath the soil, (2) the position of these old channels and - their depth, (3) the kinds of rock in the valley, (4) their character for construction and permanence, (5) the possible interference of underground water circulation, (6) the possible excessive losses of water through porosity of strata, (7) the proper depth at which the tunnel should be placed, (8) the kinds of strata, and their respective amounts that will be cut at the chosen depth, (9) the position and character of the weak spots with an estimate of their influence on the practicability of the tunnel proposition. Then after these have all been considered the whole situation must be interpreted -and- translated into such practical engineering terms as whether or not the tunnel method is practicable, and at what point and at what depth it should cross the valley, and at what points still further exploration would add data of value in correcting estimates and governing construction and controlling contracts. This is a general view of one case, the first one of any large proportions in following down the aqueduct. - There. are. many others. In nearly all of them the importance of geologic. questions is prominent. Many of them, of course, are of the simplest sort,: but, on the other hand, some are among the most obscure and evasive problems of the science. And they do not become::any (A]ddug 190jeAQ JO pavog Ai} YIOA MON Aq ydeisojyoyd) ‘s[[P{syeD ey premo} oSurl YUNSULALYS IY} Jo ULSIVUU OY} WOsF OUT, JONpen be oy} Suo[e YOU SUIyxOO| Ad][eA JNOpUoY IY} JO MoIA [V1OUT) pero —nree cee een GEOLOGY OF THE NEW YORK CITY AQUEDUCT 19 easier simply to know that they must ultimately be stated in terms precise enough for the use of engineers, and to know furthermore that the real facts are to be laid bare when construction begins and as it progresses. But from another viewpoint it may be regarded as an exceptionally fine opportunity to study applied geology in its best form and to see the intimate interrelationship between an engineering enterprise of great public utility and a commonly con- sidered more or less obscure science. The services of geology have been seldom so consistently employed in earlier undertakings of similar character. It is to be hoped that the accompanying illus- trations of the practical application of geologic knowledge and facts to engineering plans and practice may add to the appreciation of the commonness and variety of such service in many everyday affairs. Furthermore, this unique enterprise, the like of which for magnitude and complexity has never before been attempted, has given to those whose good fortune has brought them into working relations with its problems, the opportunity of a generation in their chosen field? The success stages from isolated observations, inference, hypothesis, theory, conclusions, and fully proven facts are all represented. The steps more or less fully coincide with the degree of confidence observable in the tone of advisory reports to the engineers in charge — representing suggestions, recommenda- tions, or specific advice. It is one of the cherished wishes of the writer of this bulletin that some of these problems may be presented in such manner as to serve a distinct educational purpose. For this reason in part, deeming it even of greater importance than the mere enumeration of newly discovered facts, the writer has chosen to treat the sub- ject from the standpoint of an instructor illustrating the develop- ment of working conclusions. - It is certain that not all readers have the same degree of preparation or acquaintance with the subject- matter, and it may therefore be useful to include many things that some may well pass by. No excuse is offered except that such method of treatment, in behalf of the general intelligent public that it is hoped to reach, seems to the author to be advisable. 1 W. O. Crosby of the Massachusetts Institute of Technology, James F. Kemp and Charles P. Berkey of Columbia University have constituted the staff of consulting geologists throughout most of the exploratory work. 20 NEW YORK STATE MUSEUM Other problems The foregoing observations apply likewise to the other larger problems of the aqueduct line. A list of the larger ones requiring extensive exploration and illustrating geologic application in their solution are given below: 1 Location of the Ashokan dam 2 Sources of material for construction 3 Crossing the Rondout valley 4 The Wallkill valley 5 Moodna buried valley 6 Pagenstechers gorge and Storm King mountain 7 The Hudson river crossing problem 8 The Storm King-Break Neck cross section g Foundry brook 10 Sprout brook notch 11 Peekskill creek valley 12 Croton lake pressure tunnel 13 Bryn Mawr siphon 14 The new Kensico dam 15 Kensico quarries 16 New York city delivery tunnel In addition to these there are several questions of general bear- ing in which the chief lines of argument and the chief basis of con- clusion are essentially geologic. Although little wholly new data is yet available on these particular questions from any direct work of the aqueduct, yet it will add materially to an appreciation of the far-reaching influence of established geologic data and geologic rea- soning to enumerate some of them: 17 Continental subsidence and elevation 18 Crustal warping 19 Postglacial and present faulting 20 Underground water circulation 21 Relative resistance of the different formations to corrosion by aqueduct waters 22 Structural materials Each of these problems or questions or topics is discussed sepa- rately, so far as practicable. By adopting this plan, of course there is a tendency to repetition but this to a certain extent is unavoid- able. Some of it is overcome by suitable references to preceding GEOLOGY OF THE NEW YORK CITY AQUEDUCT 2! discussions. Where such cross reference is too cumbersome, the items are repeated in preference to leaving the case obscure. Thus it is hoped to make each case a unit, and the whole series useful and understandable. Gathering data In the accumulation of data all the members of the engineering corps: as well as the men acting only in a consulting capacity have taken part. Necessarily the bulk of the exact data has been gathered by the men all the time on the ground and whose duty it was to superintend explorations. The care and intelligence with which this has been done is notable. A considerable proportion of the labor of manipulating the accumulated data and interpreting it so as to reach an explanation of conditions and formulate conclu- sions has been assumed by the consulting men. Too much credit can not be given to the heads of departments and divisions for the open-handed way in which all needed facts were held available at all times for comparison and guidance toward sound conclusions. The information upon which investigations have been initiated have been chiefly the following: 1 The geologic maps and reports of the New York State Survey 2 United States topographic maps 3 Geologic folio no. 83, New York city folio 4 Earlier engineering records and reports 5 Reports of special commissions on water supply 1 In this work, no group of men have had so direct responsibility as the division engineers. The success with which so many complicated explora- tions were carried out is chiefly due to their constant care and foresight and perseverance and the able assistance of their staff. Those who have had especially important divisions for the geological problems involved are given due credit in the discussions of part 2, of this bulletin. It is easy, how- ever, to neglect sufficiently full acknowledgment of their services in gather- ing and formulating data of this kind. Among those having charge of the most important exploratory work the following names should appear: James F. Sanborn, for sometime assigned to geologic work on the North- ern aqueduct. William E. Swift. in charge of the Hudson river explorations. William W. Brush, in charge of the early New York city explorations. Lazarus White, in charge of the Rondout valley explorations. Lawrence C. Brink, in charge of the Wallkill division explorations. J. S. Langthorn, in charge of the exploratory work at the Ashokan Reser- voir. Wilson Fitch Smith, in charge of work at Kensico dam, and A. A. Sproul, in charge of the Peekskill creek and Sprout brook explora- tions. 22 NEW YORK STATE MUSEUM Some of these are printed reports and records not directly con- cerned with this enterprise, but whose information has been found useful in this field. This is especially true of the first four sources enumerated, I, 2, 3, 4. The last is a specific study with direct reference to this project. Investigations were begun from the above vantage point. The methods employed and the explorations conducted constituting the further sources of information and furnishing the complete data upon which all conclusions have been based include the following: 6 Detailed topographic studies of the engineers of the Board of Water Supply Geologic field work making observations in detail of all geo- logic factors that seem to bear onthe problem in hand Wash borings for depth to bed rock Chop drill holes through stony ground to bed rock 10 Shot drill holes in bed rock Ir Diamond drill holes 12 Test pits and trenches for detail of drift structure 13 Test tunnels in rock for working quality 14 Deflection tests for holies that have swerved aside 15 Pumping tests for underground water supply 16 Pressure tests for rock porosity 17 Microscopic examinations of rock types 18 Laboratory tests of quality and behavior of materials. a | Oo © The mass of data accumulated from all these sources is surpris- ing. For example, there are upward of 200 wash borings on the different proposed Hudson river crossing lines alone; there are 69 drill borings and 177 wash borings on the site of Kensico dam: there are 69 shot and diamond drill holes on the Rondout siphon line aggregating 10.234 feet of rock core; there are 65 drill holes of various sorts on the Moodna creek siphon aggregating in total pene- tration of drift over 10,000 feet: there are 106 borings, besides several pits and trenches at Ashokan dam location. At every point explorations suitable to the particular problems in hand were con- ducted. The whole mass of data is conveniently recorded, much of it is tabulated, some of it is represented graphically, samples of nearly all of the material are available for examination? and all 1The cores of all drillings and suitable samples of all borings in drift have been saved and properly labeled and are to be permanently housed at some convenient point on the aqueduct line when completed. At present they are cared for at the different division offices. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 23 have been made use of in coming to a consistent understanding of the conditions. But the amount of accumulated data is no more remarkable than the difficulties that have been encountered in obtaining it. For example, in the Moodna valley it has taken three to four months’ time to put down a single hole to bed rock — the average time con- sumed for each of the 15 holes exploring the deepest portion of the valley was about 60 days. The chief trouble is caused by heavy bouldery till. In one case a boulder was penetrated for 35 feet. lying a hundred feet above bed rock. The extreme of such difficulty is, of course, encountered in the Hudson river itself, where the drill has to contend with: (1) the rise and fall of the tides, (2) the river currents, (3) a maximum of go feet of water, approximately 700 feet of silt, gravel, till, boulders, etc., filling the old preglacial gorge. The heavy steamboat and towing traffic has been a serious element in the problem. Probably never anywhere have drillmen had to face so nearly insurmount- able obstacles. In two years only two holes reached below a depth of 600 feet below sea level. A third, now in progress, has pene- trated a depth of 768 feet without entering rock. hy ae. AD ate * Maite ‘7 ; &e may CHAPTER ill RELATIVE VALUES OF DIFFERENT SOURCES OF INFORMA- TION AND STAGES OF DEVELOPMENT In the earlier stages of work topographic features were of most concern, and they largely controlled the selection of reservoir sites and possible lines for the aqueduct to follow. It was, however, at once recognized that tunnels would be unavoidable and studies as to the types of rock formations to be encountered were begun It was also early appreciated that the soil or drift cover is very unevenly distributed over the rock surface and that, especially in the chief valleys requiring pressure tunnels, it would be necessary to determine the profile of the rock floor. At this point wash bor- ings were begun. But the natural limitations of the wash rig’ for penetrating drift of all kinds left the information still too indefinite. The wash rig can not penetrate hard rock. It can not wash up anything but the finer matter, and a boulder of very moderate size is almost as effectual a barrier as true rock ledge. By a combination of washing and chopping or by the use of an explosive to break or dislodge an obstruction some progress in unfavorable material may be made, but the wash rig alone, in a drift-covered region, gives only negative results. It is certain, for example, that bed rock lies at least as deep as the wash rig has penetrated, but it is not certain that it is bed rock instead of some other obstruction. Except in areas of special drift conditions,? therefore, the wash rig was insuf- ficient. To rely upon the process at random was clearly impossible, and to determine whether or not the results of a particular locality 1A “wash rig” is a device composed essentially of two iron pipes, one within the other, and so mounted that the inner one can be worked up and down in sort of a churning fashion while water under considerable pressure is forced through it to the bottom and out again by the larger pipe to the surface, carrying up with the current the displaced sand and clay. As progress is made with the inner pipe the outer one is from time to time driven down and the process renewed and repeated till the hole is finished. 2One of the most notable areas of special drift conditions is repre- sented in the Walkhill valley lLsee discussion in pt 2] where there were developed large deposits of modified drift, stratified gravel, sand and clays, lying immediately upon the bed rock floor. In this the wash bore process was eminently satisfactory, and the rapid progress made by it together with its economy made this an especially attractive method of exploration. [25] 26 NEW YORK STATE MUSEUM could be relied upon became involved at once with an interpretation of local glacial phenomena, especially an interpretation of the char- acter of the local drift. In order to see the limited application of this method one needs only to point out that the majority of drift deposits in this region are stony or even bouldery, forming thick coverings in the valleys, and to call attention to the experience at two or three points. For example, at Moodna creek, the prelimi- nary wash borings were obstructed and bed rock reported at 5 to 15 feet below the surface where afterward, by other means, it was proven to lie more than 300 feet down. Or again, in the pre- liminary wash borings in the Hudson, the rigs were stopped and rock bottom provisionally reported at from 25 to 200 feet below sea level, but later explorations have proven at the same point that rock bottom is more than 700 feet down. Therefore, to the “ wash rig” was added the “chop drill” and the “oil-well rig” and to these, or to modifications of them,’ the success in reaching bed rock has been due. | From independent field studies of a more strictly geologic nature it became clear that many of the valleys, where pressure tunnels were proposed, are of comparatively complex geologic structure and exhibit considerable variety of rock quality and condition. This then introduced and necessitated still more elaborate lines of ex- ploration. It was not enough to know the profile of rock floor alone, it became of equal importance to penetrate the rock and obtain samples of it. So the shot drill? and the diamond drill* were employed and the drill cores preserved for identification and reference. 1 The essential features of the machines in most instances are, a high tower or support, a heavy chisel-shaped plunger that can be raised by a rope and dropped repeatedly in the hole, destroying or displacing obstructions, and which can be followed by a casing driven down as progress is made—a combination of washing, chopping and driving. 2 The shot drill, or calyx drill, is essentially a machine devised to rotate a steel tube which is so adjusted and manipulated that a supply of small chilled shot can be kept continually under the lower end as it bores into the rock. The cutting is done by the shot immediately under the edge of the tube. A core remains in the tube and may be recovered. Its best position is vertical. 3 The diamond drill consists essentially of a bit or crown set with black diamonds (bort) in such manner that when the bit is attached to a rotating tube a circular groove is cut into the rock. By proper attachment to jointed tubes and driving gear a hole may thus be bored at any angle and to great depth and a core recovered. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 27 _ These preserved cores, now aggregating many thousands of feet have been of great service in determining the precise limits of formations and consequently the geologic structure or cross section, by which detailed estimates may be guided. Even these occasionally appeared to give insufficient data. The peculiar behavior of certain holes, as, for example, one or more at Foundry brook, led to the suspicion that the drill had swerved from its course, following a particularly soft seam or zone, and that the results secured by it without large corrections, were wholly misleading. Tests proved that there had been a deflection. At this and many other places it later became very desirable to form some quantitative as well as qualitative opinion of the condi- tions existing in the underlying strata. The percentage of core saved, the rate of progress of the drill, the behavior of the drill, the condition of the core recovered, the loss of water in the hole — all these of course were considered. For more definite evidence as to porosity and perviousness, a series of carefully planned pressure tests? were made. By shutting off connection with the walls of the hole above a certain stratum and forcing water in under pressure, it was possible to demonstrate that certain strata or certain portions were practically impervious in their natural bed, while others were much less so, and:to get an idea of their relative efficiency as water carriers. For the pressure tunnels, especially, this test is a very suggestive line of investigation. 1 At Foundry brook [see discussion of this problem in pt 2], the remark- able condition apparently shown was a reasonably substantial ledge of granitic gneiss, so feet, followed below by 200 feet of apparently soft sand and reported as such. No core could be recovered. So extensive a zone or bed or layer or mass is hardly conceivable considering the crystalline silicious character of the rock. It probably represents a steepiy dipping crush zone along fault movement where the increased underground circulation has been unusually effective in producing decay. After enter- ing this zone the drill swerved from its initial course and kept within the soft seam. 2 The pressure test is made by means of a force pump, fitted with a gage on which the pressure is recorded, connected by a pipe to the por- tion of the hole to be tested, and so adjusted to a device for blockading or damming the hole that the water pressure is confined to those portions of the walls of the hole below the dam, or between two dams if an upper and lower one are used. In this way any portion of a hole, or stratum or several beds together may be tested and the amount of water absorbed per unit of time per unit of pressure determined. This is, of course, directly related to the porosity of the rock and is approximately inversely proportional to its presumed value as an aqueduct carrier. 28 NEW YORK STATE MUSEUM Where the strata are especially porous and where underground or permanent ground water supplies are very extensive and where at the same time the largest or deepest pressure tunnels are projected some uneasiness has been entertained as to the extent of interference from inflowing water during construction. An attempt to form some idea of the ease of such underground circulation has been made by a systematic pumping of one or two critical holes. The results leave many factors still too obscure to draw definite con- clusions. The test will be taken up again in the discussion of the Rondout siphon in part 2. | Laboratory tests and experiments on materials complete the list of lines of investigation with which this bulletin is concerned. Although from the nature of the case these are elaborate and unusually complete, the more important lines are not at all new. _ All the methods of petrographic, chemical, and physical manipula- tion that seem to promise practical results of value to the success of the undertaking are followed and the data are organized and interpreted and conclusions are formulated with as great definite- ness for practical bearing as other lines of investigation. CHAPTER IV GENERAL GEOLOGY OF THE REGION It will save much repetition and it is believed will altogether serve a useful purpose in maintaining unity of treatment to give an outline of the geologic features of the region in advance of the discussion of special problems. It is intended only for those not sufficiently familiar with the general geology to follow subsequent matters. The region includes some of the most complicated and obscure sections of New York geology. It is simple in almost no one of the larger branches of the subject. In physiography there is the long and involved history and the results of long continued erosion of a variable series of formations in different stages of modification as to structure and metamorphism and attitude, modified still fur- ther by subsidences and elevations, depositions and denudations, peneplanations and rejuvenations, glaciation and recent erosion — all together introducing as much complexity as can well be found in a single area. In stratigraphy the whole range of the eastern New York geologic column is represented from the oldest known formation up to and including the Middle Devonic —a succession of at least 25 distinct formations which may for convenience be treated in groups that have had similar history. Each of these formations has a constant enough character to map and regard as a physical unit. Even this classification ignores the great range of petrographic variability shown in stich formations as the Highlands or Fordham gneisses. All but two or three of these formations will be cut by the tunnels of the aqueduct. In petrography the range is even greater — so great, in fact, that only an enumeration of the variations will be attempted. They include clastics, metamorphics and igneous types; stratified and un- assorted, coarse and fine, detrital and organic, marine and fresh water, homogeneous and heterogeneous, argillaceous, calcareous and silicious sediments, unmodified and thoroughly recrystallized strata ; acid and basic and intermediate intrusions; massive and foliated crystallines — of many varieties or variations in each group. In tectonic geology an equal complexity prevails. There are regu- lar stratifications, cross-beddings, disconformities, overlaps and un- conformities ; interbeddings, lenses and wedges; flat, warped, tilted [29] 30 NEW YORK STATE MUSEUM and crumpled strata; monoclinal and isoclinal, open and closed, anticlinal and synclinal, symmetrical and overturned, horizontal and pitching folds; joints, crevices, caves, crush zones, shear zones, and contacts; normal, thrust, dip, strike, large and small faults; veins, segregations, inclusions, dikes, sills, bosses and bysmaliths. With such variety of natural conditions it is not surprising that the problems of the aqueduct are also of great variety. No two have in all respects the same factors in control and no two can be explored and interpreted upon exactly the same lines. 1 Geographic features or districts. (Physical geography’) It will be convenient at this point to think of the surface topog- raphy by districts — not wholly distinct from each other, but still with essential differences of origin and form. From south to north they are: (a) New York-Westchester county district. The area of crystalline sediments. South of the Highlands. (6b) Highlands of the Hudson (Putnam county). (c) Wallkill-Newburgh district. From the Highlands to the Shawangunk range. (d) Shawangunk range and Rondout valley. (e) Southern Catskills. All have been sculptured by the same forces and with similar vicissitudes, but the difference of history and structure and condi- tion, already established when the physiographic forces began on the work now seen, have caused the variety of surface features indi- cated in the divisions made above. The more noticeable character- istics of these five districts are here given. a New York-Westchester district. The area south of the Highlands proper is characterized by a comparatively regular suc- cession of nearly parallel ridges separated by valleys of nearly equal extent (% to 5 miles wide), making a surface of gently fluted aspect and of moderate relief (0-500 feet) sloping endwise toward the Hudson and the sea. The controlling factors in producing this topography are involved in a series of folded, foliated, crystalline sediments, of differing resistance to destructive agencies. b The Highland region is one of rugged features, with a range of elevation of o-1600 feet A. T., forming mountain masses and ridges separated by very narrow valleys all having a general northeast and southwest trend across which the Hudson cuts its way in a narrow, angular gorge, forming the most constricted and crooked portion of its lower course. The bed rock is all crystalline, 1 The physiographic history of a region is not understandable without a comprehensive knowledge of its geologic features and structures and history. It is therefore treated in a later paragraph. (Ajddng 103¥\A\ fo preog oy} Aq ydeisojoyg) ‘“punoisyoeq 9} Ul S{[Iysied oY} YIM JOULISIP oY} UL AodT[vA Jno -puoy oY} pure PUNOLSI10F OY} UL DY] YUOYOPT YIM osuvt YUNSueMeLYS oY} Ul doy AYS WoOIZ JSOM Bulyoo, Mop "i 4 on aes t —_ * Py . ~ “ 2 . GEOLOGY OF THE NEW YORK CITY AQUEDUCT 31 oi massive and foliated types, metamorphosed sediments in part with large masses of igneous intrusions and bosses. c The Wallkill-Newburgh district lying immediately north of the Highlands and extending to the Shawangunk range is a region of gently rolling contour. Most of the area along the pro- posed lines lies between 200 and 500 feet above the sea. ‘There are only occasional rugged hills or short ridges, such as Snake hill and Skunnemunk. The valleys are broad and smootn and the divides are simply broad, hilly uplands. Bed rock is chiefly Hudson River slates with occasional belts of Wappinger limestone. The larger features, the trend of divides and valleys, are northeast and south- west, although this regularity is not so marked as in the preceding two districts. But the chief streams flow either northeast or south- west to the Hudson along these general lines. d The Shawangunk range and Rondout valley form a transitional unit from the complicated structural and tectonic con- ditions of the southerly districts to the uniform and almost undis- turbed strata of the Catskills. Its southeasterly half is a mountain ridge partaking of extensive faulting and folding and represented by the Hudson River slates overlain unconformably by the thick and very resistant Shawangunk conglomerate forming high east- ward-facing cliffs. Toward the northwest these disturbances dimin- ish, the strata gradually pass deeper beneath a great succession of shales, limestones, and sandstones of the Helderbergian series, and a broad valley is eroded in the softer portions. It is limited on the northwest by the prominent and very persistent escarpment border- ing the Hamilton series and forming the outer margin of the Cats- kill mountains. e The Catskill area is of simple structure. The strata are well bedded and lie almost flat with a gentle dip northwest. The surface features form a series of irregularly distributed escarp- ments, hills, valleys, cliffs, gorges and mountains, rising rapidiv toward the west, with moderate to strong relief and reaching ele- vations of 2500 feet. The failure of the northeast-southwest trend of feature that is so common in all of the other districts is a marked difference. It is directly due to the flatness of the strata. 2 Stratigraphy There are no strata of prominence in association with the main aqueduct younger than Devonic age except the glacial drift. Imme- diately adjacent areas, however,-some of which are covered by the accompanying maps, and Long Island have later formations ex- 32 NEW YORK STATE MUSEUM tensively developed. Such are the Triassic rocks of the New Jersey side of the Hudson below the Highlands, and the Cretaceous and Tertiary strata of the Atlantic margin on Long Island and Staten Island. The development of underground water supply on Long Island is especially concerned with these later formations, and with the modified drift deposits of the continental margin. The whole series of formations are more commonly considered in groups that exhibit certain age or physical unity and that are for the most part characteristic of certain regional belts and that coincide somewhat roughly with the physiographic divisions already noted. There is in the following description and tabulation no direct attempt to unduly emphasize this relation or to belittle the divisions recognized in the commonly adopted geologic column. It is, how- ever, for the purpose in hand, more convenient and useful to keep clear the physical groupings, because largely these groups, instead of the more arbitrary subdivisions of age, are the units used in con- sidering structural and applied problems. | a Quaternary deposits. (1) Glacial drift. A loose mantle of. soil and mixed rock matter covers the bed rock throughout the whole region except (a) here and there where the rock sticks up through (outcrops), and (b) at the most southerly margin along the coast where the glaciers seem not to have reached. Origin. This mantle is usually very different in lithologic charac- ter from the underlying rock floor. There is almost always an abrupt break between the rock floor and the overlying material. The rock floor is grooved, smoothed, and scratched as if by the moving of rock or gravel over it. The larger boulders are usually of types of rock identical with ledges lying northward at greater or ‘less distance. Materials of exceedingly great variety both in size and condition and lithologic character are often all piled to- gether in the most hopelessly heterogeneous manner. These are now commonly regarded as conclusive evidence of glacial origin. There is no need of making the discussion exhaustive. It is almost universally called the “ drift.” Thickness. The thickness of the drift varies from almost 0 to ap- proximately 500 feet. It is generally thickest in the valleys where it has simply filled many of the original depressions and obliterated much of the ruggedness of surface, the gorges and ravines and can- yons of the preglacial time. Sources. It appears from an examination of the grooves and striae on bed rock, and the relationship of the different types of drift to each other, and from a comparison of the types of boulders * * GEOLOGY OF THE NEW YORK CITY AQUEDUCT 33 with the ledges that may be regarded as their source, that the gen- eral ice movement was from north to south swerving along the southerly extension to east of south. Therefore it is not unusual to find abundant boulders of Palisade trap stranded in New York city or on Long Island, or boulders of the Cortlandt series, or of the gneisses of the Highlands, or, in occasional instances, of sand stones from the Catskills, or the limestones from the Helderbergs or perhaps in rarer cases even rocks from greater distance, as the Adirondack mountains. Kinds of drift. There are in the region two fundamentally differ- ent types of drift as to method of deposition. They are (a) unas- sorted drift (till or hardpan), and (b) modified drift (stratified or partially assorted gravels, sands, clay, etc.). The former (a) repre- sents deposition directly from the ice sheet at its margin (terminal Or marginal moraines) or beneath (“ground moraine”) without enough water action to rework and assort the material. It there- fore contains boulders, pebbles, sand and clay of a heterogeneous mixture of the most complex sort both as to size and character. In such deposits there is almost always sufficient intermixture of clay and rock flour of the finest sort to make a very compact and dense mass that is usually quite impervious to water. Such deposits are distributed rather unevenly over the surface and where this uneven- ness leaves hollows or basins, or obstructs the outlets of other de- pressions, they may hold water and form small lakes or ponds or swamps. This is almost universally the origin of the many thou- sands of lakes of the northern lake region. It is evident that ma- terial of this character, a type that commonly serves the purpose of a natural dam or reservoir, would be especially important and useful at certain places on the Catskill system. As a matter of fact, so far as geologic features are concerned, it is the chief factor in choice of location for the Ashokan dam [see discussion pt 2] and is a con- trolling factor in the plans for the erection of the miles of dikes at less critical margins of the reservoirs. Till is an extensively developed type but frequently passes abruptly either laterally or vertically into assorted materials of very different physical char- acter. (6) All materials associated in origin with the glacial occupation that have been materially modified especially in the direction of an assorting of material are referred to as “ modified drift ” deposits. They include (1) deposits made by both water and ice together, (2) those fermed by running water, (3) those laid down in stand- 34 NEW YORK STATE MUSEUM ing water. Or again (1) those accumulated rapidly with very irreg- ular supply of material at the margin of the ice-forming, hummocky or hill and kettle surface (kames, eskers), (2) those carried along valleys or general lines of drainage to a considerable distance beyond the ice margin aggrading the valley with the overload of gravels and sands (valley trains), (3) those washed out from the ice margin iu more even distribution forming a gently sloping and thinning extramarginal fringe (outwash or apron plains), (4) those fine matters that are carried by glacial streams into the margins of more quiet waters, either a temporary or a permanent lake or a larger and slower stream or other body forming more perfectly assorted and more evenly stratified deposits (delta deposits), (5) those finer rock flours and clays that remain suspended longer and carry out much farther settling only in the very quiet waters of lakes ov estuaries or temporary water bodies of this character forming the perfectly banded clays (glacial lacustrine clays). It is evident then that modified drift has in the process of its accumulation suffered chiefly a separation of fine from the coarse particles and that in most cases the fineclay filling that makes the till dense and impervious to water, has been washed out and de- posited by itself in the more inaccessible deeper waters. As a re- sult most modified drift deposits are pervious.and easy water conductors, but poor or questionable ground for dikes or dams or basins [see discussion of Ashokan dam, pt 2]. | Some of them, the medium sands and gravels, furnish an excel- lent and already cleaned structural material for concrete or mortar, such as the Horton sand deposit, or coarser kinds may be crushed — and sized before using as is done at Jones Point on the Hudson. The finer silts and clays, usually overlain by assorted sands, are abundant along the Hudson, having been deposited there at a time when the water of this estuary stood 50 to 150 feet higher than now. Recent erosive activity of the river has cut the greater pro- | portion of the original deposits away but at many places large quan- ~ tities still remain above water level in the banks and still greater _ quantities extend beneath the river. These deposits are the support of the brick industry of southeastern New York. The till deposits are very difficult to penetrate in making borings because of the boulders, the wash rig being almost useless. Modified drift of the ‘medium and finer sorts is easily and cheaply penetrated, and, if it — i lies on bed rock, such exploration gives reliable results. Structure. But this is stating the actual conditions too simply. | The glacial epoch was a complex one The continental ice sheet may GEOLOGY OF THE NEW YORK CITY AQUEDUCT 35 have advanced and retreated repeatedly, how many times in this region is not clear. Wa5th each time of advance and retreat, the work done by it partly destroyed, or disturbed or modified or cov- ered the earlier ones in what appears now to be a most arbitrary way (in reality, of course, in a very consistent way for the condi- _ tions that then existed). So one frequently finds a till beneath a de- posit of stratified drift, or modified drift beneath till, or a succession of a still greater number of changes in almost hopeless confusion. In New York city, for example, at Manhattanville cross valley, the exposed drift above street level includes (a) at the bottom, water-marked stony till and assorted gravels, (b) in the middle per- fectly horizontal, stratified rock flour and the finest sand, (c) top, wholly unassorted bouldery till, covered by thin soil. It is evident that the most careful and accurate identification of the surface type without subsurface investigation would give, for such uses as are now being considered, thoroughly unreliable evidence as to the behavior of the whole body at this point. Therefore, a determina- tion of the changes and quality forms an essential record. All of these types are to be found in the region, but the different grades of till and roughly modified material belonging to the kame type are more common inland. On Long Island the development of marginal modified types is extensive and more or less obscured by the advance and retreat noted above. The larger divisions recognized in deposits are (a) an early accumulation of sands and gravels, strongly developed near the western end of the island, known as the “ Jameco” gravel, (6) an interglacial (retreatal) deposit of blue clays known as the “Sankaty ” beds, (c) a later series of deposits, sands, clays, gravels and till, belonging to the closing stages of the ice period correspond- ing to the surface deposits of the larger portion of the whole region (Tisbury and Wisconsin advances). Some of these sands and gravels are important water-bearing sources for the new Brooklyn additional supply. ; The whole Long Island series according to Veatch?! includes: Glacial 1 - acial two lines of ter See pig cretite Wisconsin stage [ minal moraines with out- Ronkonkoma moraine - ( wash plains Great deposit of outwash sand and gravel (de- Tisbury stage pression ) Gardiner interval with erosion (interglacial) 1 After PP 44, U. S. Geological Survey, p. 33. 2 36 NEW YORK STATE MUSEUM ¢ Folding (glacial folding) Sankaty retreatal stage (interglacial) clay beds Glacial — Jameco gravels Postmannetto erosion (interglacial) Mannetto stage Glacial — old gravels Gay Head Jameco A radically different and in some respects a much simpler inter- pretation’ of the Long Island deposits has been outlined by W. O. Crosby. The essential feature of his classification is the unity and simplicity of the glacial epoch. Only the moraines and associated sands and gravels of outwash origin during advance and retreat are regarded as glacial. All other deposits below and including the sSankaty clay beds he regards as preglacial. _ The Jameco gravels are interpreted as Miocene in age. Certain persistent yellow gravels overlying the Jameco are classi- fied as Pliocene. 6 Tertiary and Cretaceous deposits. (2) Tertiary outliers. Deposits of Pliocene age are littoral in type [PP 44 U. S. G. S. p. 28] and are not very well differentiated (Long Island, Staten Island). Probably equivalent to the Bridgeton beds of New Jersey. Certain “ fluffy” sands in thin beds are assigned by Mr Veatch to the Miocene (Long Island, Staten Island). Probably equivalent to the Beacon hill deposits of New Jersey. Crosby places the Jameco gravels in the Miocene together with the Kirkwood lignitic and pyritic clays and sands. (3) Upper Cretaceous deposity? are extensively developed. They form the chief bed rock of Long Island. 1 The writer offers both of these outlines of the glacial and associated deposits in preference to either alone. Both Veatch and Crosby have given immensely more time to the study of these questions than any one else. It is hardly fitting for a newcomer in their field to reject either view. But because of the very great difference between the two interpretations one may be pardoned a preference. It is the writer’s opinion that the simpler outline is the more tenable. It does not seem possible to establish a very complex series of stages in the glacial epoch as represented in the deposits of southeastern New York. 2 Crosby’s classification of the Cretaceous is as follows: (a) Monmouth — slight development of marls. (Lower and middle marl series.) (b) Matawan — (clay marl series) probably present on Long Island. (c) Magothy —an extensive series of variegated and micaceous sants and clays. Heavy development on Long Island. (d) Raritan — Plastic clay scales and the Lloyd sand. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 37 (a) A lignitiferous sand with occasional clay beds forming the uppermost of the Cretaceous series is probably equivalent to the marl series of New Jersey. But it lacks the prominent greens and development characteristic of the region further south. Not clearly separable from the underlying formation or Matawan beds. (b) The Matawan beds. Gray sands and clays. (c) Raritan formation. Clays and sands, plastic clays, the Lloyd sand, an important water carrier lies about 200 feet below the top of the formation. Occasional leaf impressions. All of these formations, except where disturbed locally by glacial ice, dip gently seaward. The sand beds of these strata are the chief sources of underground water being developed by the new system. c Jura-Trias formations. (4) Palisade diabase. This is a thick intrusive sheet, or sill, of igneous rock of diabasic type. It is 700-1000 feet thick. It lies for the most part parallel to the bed- ding of the surrounding, inclosing, sedimentary rocks, and, rising gently eastward, forms a strong cliff continuously along the west bank of the Hudson for 40 miles. It varies from very fine to very coarse texture and is for the most part fresh, tough, durable, and is the source of large quantities of the most satisfactory quality of crushed stone now on the market for use in concrete. (5) Newark series. This is a very great thickness of silicious sediments, chiefly reddish conglomerates, red and brown quartzose and feldspathic sandstones and shales. They dip gently westward and northwestward at 10-20 degrees, and are confined, in this region, to the west side of the Hudson south of the Highlands. The formation supplies “ brownstone” for building purposes. None of the Jura-Trias rocks, so far as known, will be cut by the aqueduct. d Devonic strata. (6) Catskill formation. This formation’ is of continental type, chiefly a conglomerate. A white conglomeratic sandstone forming the uppermost portion attains its greatest thick- ness on Slide mountain (350 feet). It is a “ coarse grained, heavy bedded, moderately hard sandstone containing disseminated pebbles of quartz or light colored quartzite, and streaks of conglomerate.” A red conglomeratic sandstone constitutes the much thicker por- tion below (1375 feet). It is a “ coarse, heavy bedded sandstone of dull brownish hue containing disseminated pebbles and conglom- eratic streaks, differing from the overlying beds chiefly in color. In 1Grabau, A. W. N. Y. State Mus. Bul. 92. Geology and Paleontology of the Schoharie Valley. . 28 NEW YORK STATE MUSEUM both series the pebbles and conglomeratic streaks are scattered and irregular, while the sands are often cross-bedded. Thin layers of red shale occur, and locally gray sandstones.” The deposits prob- ably represent flood plains, deltas, and alluvial fans accumulated mostly above sea level. (7) Oneonta sandstone (Upper flagstone). “Thin and thick bedded sandstones from 20 to 200 feet thick with interbedded red shales up to 30 feet thick.” Chiefly light gray to brown in color. Abundant cross-bedding, occasional dark shale, frequent flagstone beds. Capable of furnishing “ bluestone” flags and more massive dimension stone. To be seen in the vicinity of West Shokan and westward. (8) Ithaca and Sherburne (lower flagstone “ bluestone”). “ Thin bedded sandstone, with intercalated beds of dark shale. The sand- stones are in masses from a few inches to 40 feet in thickness, greenish gray to light bluish gray or dark gray in color, and are extensively quarried as flagstones.” There are occasional conglom- eratic streaks. Occurs in large development in the vicinity of the Ashokan reservoir (500 feet). The heavier cross-bedded and coarser grained beds are capable of furnishing an unusually good quality of large dimension stone for heavy structural uses. The beds of this formation near Olive Bridge will in all probability furnish the greater proportion of stone of all kinds for the con- struction of the great Ashokan dam [see discussion of bluestone near Ashokan dam, pt 2]. The chief common fossil content is impressions of plant remains. | (9) Hamilton and Marcellus shales. “ Dark gray to black or brown shales with thin arenaceous beds in the upper part.” Forms the upper portion of the escarpment that follows the outer margin of the Catskill foothills bordering the westerly side of the middle Rondout and lower Esopus valleys. Occasionally beds are sub- stantial enough for flagstone production (700 feet or more with the Marcellus. ) | The) chief ‘index “fossils are? Sipiiifex a epee eis Athyris .spiriferoides,, "Clhonemeshee miosis tue The Marcellus shale is not readily differentiated in the Esopus valley. Characteristically it is a thin bedded shale of no great thickness (180 feet in the Schoharie valley) lying between the Onondaga limestone and the Hamilton and obscured by talus from the escarpment (with the Hamilton 700 feet.) Styliolana Zissurella, (Chometes imam cro mat ws; Strophalesia trincata;, Lior hync nas angst. (Ajddng 19}eAQ JO plvog Aq ydeisojoyd) ‘osplig aAyQ Ww ssvy ousnqioys ous, < GEOLOGY OF THE NEW YORK CITY AQUEDUCT 39 The dividing lines between the different sandstones and shale fcrmations, the Oneonta, Ithaca, Sherburne, Hamilton and Mar- cellus, can not be sharply drawn in the Esopus region. ‘Together they form in a large way a rather satisfactory field unit. For specific purposes it is necessary to recognize that the lower por- tions are prevailingly shales with thin bedded sandstones while the upper portions are much more heavily bedded, the sandstones pre- Fig.2 Spirifer mucronatus (Conrad), a characteristic and abundant index fossil of the Hamilton shales of the Catskill margin vailing. The five divisions may possibly be more satisfactorily made on paleontologic characters than on physical, but in most of the advisory reports on economic and practical problems involving this district the subdivisions can not be emphasized. The whole series is essentially conformable and is very little disturbed [see report on bluestone quarries, pt 2]. (10) Onondaga limestone. A bluish gray, massive, thick bedded cherty, somewhat crystalline limestone. It is strongly marked off from the Hamilton and Marcellus above, and, because of its greater resistance to erosion, usually forms a dip slope controlling stream adjustment and ultimately inducing the development of unsymmet- rical valleys with gentle easterly slopes and clifflike westerly borders where the streams are sapping the overlying Marcellus and Ham- ilton shales. It is not sharply separable from the Esopus below but everywhere in this region graduates into it with increase of silicious 4O NEW YORK STATE MUSEUM and argillaceous impurities. Estimating the formation from the drill cores that have penetrated it, and placing the lower limit as nearly as may be at the horizon of changes from predominant lime to pre- dominant silicious content, the approximate thickness in this region is placed at 200 feet. The rock where exposed exhibits considera- ble joint development and these are considerably enlarged by the solvent action of percolating waters. This factor is considered of some importance in connection with the other limestones of the district in aqueduct construction and permanence. The Onondaga has been used as a building stone formerly sold as marble, some grades of which are good stone. On the line of the aqueduct it is confined to the Rondout and Esopus valleys. The chief fossils are: Aitrypa- reticularis, Zaphrentts ~ peo meenea Leptostrophia perplana, Platyceras dumosum Leptaena rhomboidalis, Dalmanites selenurus. (11) Esopus and Schoharie shales (a slaty grit). The Schoharie as a distinct formation is not distinguishable in this region. The very thick and comparatively uniform, gritty, black, dense, almost structureless rock is a distinct unit. It is a silicious mud rock with very obscure sedimentation markings, but showing independent secondary cleavages induced by later dynamic factors, and, on long exposed surfaces always exhibiting chiplike fragments as the result of weathering. But it is not an easily destroyed rock. In so far as the bedding is obscure and the induced structure predominates, the rock is a slate; and in so far as it is distinctly gritty (sandy) instead of argillaceous it is a grit. The formation might therefore be more accurately designated as a slaty grit. The lack of plain bedding structure makes it impossible to estimate its thickness, since the foldings or other displacements can not be allowed for; but the accumulated data of drill holes in more advantageous position indicate an approximate thickness of 800 feet. The rock is considered exceptionally good ground for the tunnel. A few fossils occur the most characteristic being Taonurus caudagalli. There are also in certain layers of limited extent, Leptocoelia acutiplicata and Atrypa spinosa. (12) Oriskany and Port Ewen transition (silicious shaly lime- stone). There is no well defined and distinct separation here be- tween the Oriskany and the underlying Port Ewen, but because of the importance and persistence of the formation in other and re- lated areas the name is held. The equivalent of the Oriskany is in this district involved with a strongly developed transition zone which in physical features is intimately associated with the Port GEOLOGY OF THE NEW YORK CITY AQUEDUCT AI Ewen as a single unit. If any distinct formation is to be recog- nized it would be on the basis of transitional faunal character, placing the fossiliferous upper 100 feet in the Oriskany transition and confining the name Port Ewen to the rather unfossiliferous and concretionary, shaly, argillaceous limestone of the lower 100 feet. Fig.3 Spirifer arenoswus (Conrad), one of the characteristic index fossils of the Oriskany occurring in the Port Ewen-Oriskany transition This transition rock is strongly bedded, argillaceous and silicious limestone, very quartzose in certain layers, but there are no exposures in this area that would be called sandstones. Fossils are abundant and show marked Oriskany peculiarities. Those of most characteristic relations are: Hipparionyx proximus, Leptostrophia magnifica, Spirifer M_mrevisant. Spirtter)renosws,. Pilatyceras modostm, Strophostylus expansus. 42 NEW YORK STATE MUSEUM (13) Port Ewen shaly limestone. The beds below those noted in the preceding paragraph are essentially argillaceous, shaly lime- stones. They vary from rather massive to thin bedded, are dark grayish in color, and have a peculiar nodular or concretionary de- velopment along certain sedimentation lines. These spots have less resistance to weather than the surrounding rock and therefore develop rows of pits along the face of an outcrop. Their size, 6 to 18 inches or more across, together with their persistence makes an easily recognized physical feature. The few fossils that are found are not very characteristic. The following should be men- tioned: Spiriter perlamellosie, In the discussion and on the maps the Port Ewen and Oriskany are treated together as a single unit as the Oriskany-Port Ewen beds. (14) Becraft limestone. Massive, heavy to thin bedded, light colored, semicrystalline to thoroughly crystalline limestone. More massive beds very pure, 94+%CaCO;. Shaly beds resemble the New Scotland which they pass into at the base. The most char- acteristic features for field iden- tification are (a) pink or light colored spots, (0b) a more coarsely crystalline condition than any of the associated strata, (c) occasional large calcite cleavages to be seen wherever a fossil crinoid base As pido- Fig.<4 Sie bee cidlatne em demeie ne ef fll S)e Sete le 40 manus eata_ Hall, the most characteristic index : Lt poser eae Beacroft limestone of the Ron=- 1S broken, (d) the Mery charac- Mit eaacre ater istic ye fOSsil, 4.75 dc euietaem ten pseudogaleata, and (e) many crinoid stems. The formation carries many fossils in addition to those given above, among which are Spirifer concinnus, Uncin- ulus’ camphellamnizs: (15) New Scotland shaly limestone. Thin bedded, dark gray to reddish sandy and shaly limestones. The rock breaks out in slabs on weathering and develops red iron stains. It has especially abundant fossils, the most characteristic of which are: Ortho- thetes woolworthanus, Spirifer macropleura. Other common ones are: Leptaena rhomboidalis, Strophonella headleyama, Ripsdemella oblatas Stropheodonta becki. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 43 (16) Coeymans limestone. Heavy bedded, dark gray, argillace- ous and flinty limestone. The characteristic features for field identification are (a2) abundant chert nodules, (b) the occurrence of coral reef structure and heads of corals, Favosites helder- Fig. 5 Spiriferf¥€macropleurfa (Conrad), the most characteristic index fossil of the New Scoti:and beds in the Rondout region beneia. 2the brachiopeds -Siteberella galéata and Mpnypa metic ular is “are, very) common. This formation has a thickness of about 80 feet and is rather distinctly separated from the underlying Manlius. The Coeymans is considered the base of the Devonic system of New York. It is Fig.6 Sieberella galeata (Dalman), the most reliable index fossil of the Coeymans limestone of the Rondout region perfectly conformable upon the underlying series and it is evident that in this region there was no important break in the progress of deposition. e Siluric strata. (17) Manlius limestone. Lime mud rock, fine textured, dense, with plainly marked sedimentation lines, gray to dark gray color. The most characteristic features in the field are (a) fine texture, (D) sedimentation lines, as if laid down in quiet waters as a lime mud, (c) solution joints sometimes enlarged to 4A NEW YORK STATE MUSEUM cavelike form into which surface streams disappear (such as Pom- peys cave near. High Falls), (d) mud crack surfaces (in lower beds), (¢) occurrence of the fossil Leperditia alta. Its abundant jointing and the tendency to develop solution cav- ities from them is considered an objectionable character. (18) Cobleskill and cement beds (limestone). It is not pos- sible without the most painstaking, comparative, chemical and pale- ontologic research to differentiate the cement layers from the inclosing beds and to assign them all to the subdivisions that are recognized in some previous publications,’ as the (a) Rondout cement (0) Cobleskill limestone, (c) Rosendale cement, and (d) Wilbur limestone. There are, however, two workable natudal ce- ment beds, both at Rondout and at Rosendale, with a nonworkable layer between each case, and also one between the lower and the next underlying formation. Whether the two cement beds at Rondout represent the Rondout and the Rosendale horizons with the Cobleskill between, or whether they should both be re- garded as Rondout with Cobleskill below, can not concern’ our present problems. And again, whether or not the two cement beds at Rondout are the same two that appear at Rosendale, or whether they are equivalent only to the upper one with a new lower bed (The Rosendale) added in this area and then with the Cobleskill between these two as claimed by Grabau, does not alter the plain fact that the whole series is a physical unit. It is a gray, rather close texture limestone, resembling the Manlius proper, and con- tains few fossils. It is perhaps even better yet to group all of these limestone beds below the Coeymans into a single unit and call it the Manlius series. (19) Binnewater sandstone. Below the Manlius cement rock series lies the 60-100 foot Binnewater. It is chiefly a well bedded quartz sandstone, almost a quartzite in the upper beds with more shale in its lower portion, in color varying from white to greenish yellow and brown. The rock is rather porous in certain beds and especially along the bedding planes and is not well recemented where crushed by crustal movements. It is confined to the Rondout valley. (20) High Falls shale.2 Greenish to red argillaceous to sandy shales. The exposures are often a brilliant red while the rock 1N: Y. State Mus. Bul. 92 (Grabau), p. 311-13; N. Y. State Mus. Bul. 80 (Hartnagel), p. 355-58; N. Y. State Mus. Bul. 69 (Van Ingen and Clark), p. 1184, 1185. 2 The term given by Hartnagle. N. Y. State Mus. Bul. 80. p. 345. UMO I € C 2) i, Sah | aut >? > ISOJOU | d ) o]e puosoy IvduU JUIUT L | 2) vogq UL G 93eId UOT role) I jJUSTUID Ye (Ajddng 10}V\\ JO pleog oY} J0J pussoy oy} JO spoeq ouUO0JSOUITT et ee ae ene oe ee (Ajddng s0}eA\\ JO prvog oy} JoZJ UMOIG “DO YL, Aq Ydeisojoyd) “suru jo poyjzott oy} pur Speq Judd oY} JO 9UO JO dip pue ssouyoTYy} 9Y} SuLMoYs “A “N ‘oyVMOUUT “OUIM JUST UOJION OY} JO JOLIO}U] 9 a ee ae ee GEOLOGY OF THE NEW YORK CITY AQUEDUCT 45 from drill cores is seldom highly colored. The protected beds are more commonly greenish in color and contain much iron sulphide. Occasional thin limestone beds occur in the upper portion at High falls —one of 4 feet forms the lip of the lower fall. The High Falls shale is confined to the Rondout valley and on the line of the aqueduct is 67-100 feet thick. (21) Shawangunk conglomerate. The Shawangunk is a con- glomerate and sandstone. The constituent pebbles are almost wholly quartz, well worn, and varying in size from that of sand to pebbles of several inches diameter. But for the most part the pebbles are small, abundantly mixed with sand, bound together by a silicious ce- ment. Rarely a true quartzite is developed and still more rarely a shaly facies. The rock is therefore very hard, brittle, and in the un- disturbed portions fairly impervious and resistant. But it suffers from crushing along zones of disturbance in folding and faulting and these zones are very imperfectly recemented. It is a durable rock, very resistant to ordinary decay, but forms great talus slopes. It is used for buhrstones (millstones), etc. It varies in thickness on the lines of the aqueduct from 280-400 feet. The rock is lim- ited in its northward extension to this district — southwestward it is much more broadly exposed in the continuation of the Shaw- angunk range. The Shawangunk completes the conformable Siluro-Devonic series down to the erosion interval at the close of the Ordovicic. © The series of conglomerates, sandstones, limestones, and shales make an imposing column approximating 3000 feet of strata differ- entiated with more or less ease into 15 separate and mapable formations and a possible 5 or 6 more with careful paleontologic work. The series begins with the capping beds of the Shawangunk range and its northward extension toward the Hudson river at Rondout and Kingston, and thence westward constitutes the rock floor while its structures control the surface configurations far be- yond the limits of the region under consideration. Immediately to the north and partly within the area here treated is the famous Rosendale cement region, the pioneer cement district of America ands for" many) years ithe ybest » producer.) Ihe «strata used are almost exclusively the upper members of the Siluric (“cement beds”) closely associated with the Cobleskill between the Manlius proper and the Binnewater sandstone. Rarely the Be- craft from the Devonic series furnishes some cement rock. f Cambro-Ordovicic formations. Between the Precambric metamorphics of the Highlands beneath and the Siluro-Devonic 46 NEW YORK STATE MUSEUM sediments of the Shawangunk range and the Catskills above, lies a series of quartzites, limestones and slates less complexly dis- turbed than the older and more disturbed than the younger series —set off from both by unconformities representing time intervals that cover both folding and erosion. They are of more than 4000 feet thickness —— how much more it is impossible to estimate be- cause of the obscurity of data in the slates. There are very few fossil forms preserved in them. The series is, however, readily and sharply separable into three formations that may be mapped upon lithologic characters alone. They are of most importance in the Wallkill valley, Moodna creek, Newburgh, Fishkill, New Ham- burg and Poughkeepsie districts. Their character, structure, and conditions have required careful consideration in the decisions on the Wallkill and Moodna siphons and in the discussions on the proposed Hudson river crossings [see Hudson river crossings, pt, 2]: (22) Hudson River slates. The upper member of the Cambro- Ordovicic series is in itself complex. Prevailingly it is a slaty shale, occasionally it is a sandstone or shaly sandstone, or a simple shale; still more rarely it is almost a true slate, and very rarely a phyllite. The constituents vary from prevailing clay to quartz sand repeatedly in almost every locality. It is probable that as a rule the upper portions are the more heavily bedded and arena- ceous. The rock is excessively affected by the dynamic movements that have at least twice disturbed it. A slaty cleavage in the more argillaceous members is most noticeable, but almost everywhere the strata are strongly tilted, crumpled, broken, faulted, or crushed in a most confusing way. This together with an original obscurity in bedding, and the obliteration by subsequent shearing of much that did exist, makes it impossible to reconstruct the complicated structure or compute the thickness of the formation. It is of such physical character as to absorb within its own limits much of the disturbing movements, and neither the formations above nor imme- diately below are so extensively and intimately affected. The formation is widely exposed and forms the bed rock over very large areas. Almost everywhere it is impervious to water, easy to pene- trate by drill or tunnel, and resistant to decay. A few Ordovicic fossils may be found, the most characteristic being Dalmanella testudinaria. (23). Wappinger limestone.1 (In part Cambric, and in part ipa Rome, © Aloe see alien a) vik ee ca a 1The Wappinger Valley limestone of Dwight (1879) and Dana. The Wappinger limestone of Darton and others. nooijuog ‘OJVIOWO[SUOD YyuNnsur (Ajddng 10}¥ A, jo pivog Aq ydessojoyq) ‘yu1od siyz t LYS St AI0L SU, “osuer yunsuemeys oy Jo syvod [}Wousq sassed jouuny dU} fo IUQ) “ORION hoojuog (A[ddng 19}e\\ fo pavog Aq ydersojoyg) ‘WorIstArp YSINGMON 24} UO UOTJONAJSUOD JONpoNnbe 19A09-puv-jnd OJ Souo}spuRS PUL sSozVIS JOATY UOSpNyT Yysnoryy Youss, y Q 31PT GEOLOGY OF THE NEW YORK CITY AQUEDUCT 47 Ordovicic). The formation is prevailingly of a compact, fine texture, dark gray, either massive or strongly bedded limestone. Where the stratification is very plain there are light and dark layers and an abundant silicious intermixture. In many outcrops the rock is sO massive that even the dip and strike are obscure. Some places the rock is fine crystalline, almost a micromarble. On weathered surfaces it almost always exhibits a crisscross etching which marks the traces of rehealed cracks. From these it is seen that many of the apparently massive compact beds have at one time been exten- sively crushed. In many places there is scarcely a square inch wholly free from these evidences. The formation is best exposed in the wide belt that extends southwestward from the vicinity of Poughkeepsie and crosses the Hudson at New Hamburg into the Newburgh district. It undoubtedly underlies the slates in the rest of the adjacent area. There are few fossils and they are rarely found. (24) Poughquag quartzite. Below the Wappinger limestone and upon the upturned and eroded edges of the Highlands gneisses lies a quartzite of variable thickness but which reaches at least 600 feet. It is a strongly silicified quartz sandstone —a quartzite by indura- tion. It is strongly bedded but seldom shaly. Traces of schistosity may appear in certain zones and this is somewhat strongly developed outside of the area at the type locality (Poughquag, N. Y.). Only fragments of trilobite spines have been found in this forma- tion within the district. g Later crystallines south of the Highlands. South of the Highlands proper except at one locality (Peekskill creek valley and its southwestward continuation through Tompkins Cove and Stony Point) the rocks are all much more thoroughly crystalline. There are two formations, and in places traces of a third, above the Gren- ville gneisses (Fordham gneisses and associates). These are known locally as Manhattan schist, Inwood limestone, and Lowerre quartz- ite. In Westchester and New York counties the quartzite is rarely found, and in a considerable proportion of those places where it does occur its relations are more consistent with the gneisses below than with the limestone-schist series above. This is true indeed of the type locality (Lowerre). There are, however, at least two points where the occurrence favors the reverse inter- pretation, so far as any is shown, and therefore a quartzite may be regarded as finishing the series, and making uncertain but probably unconformable contact with the underlying gneisses. 48 NEW YORK STATE MUSEUM This series together with the gneisses below constitutes the bed rock and controls the underground conditions for all of the line south of the Moodna valley, 50 miles above New York. All of the southern aqueduct, and the New York city distribution conduits are wholly concerned with these rocks, and two divisions of the northern aqueduct have a large proportion of their work in them. It is not wholly clear what age these crystallines represent. It is certain that the underlying gneisses are Grenville and that the metamorphic quartzite, Inwood, Manhattan series, is Post-gren- ville. It is possible that these latter are also Precambric. But usage following the correlations of Dana’ and in the absence of as good evidence from any other source has regarded them as the Cambro-Ordovicic crystalline equivalents of the Poughquag-Wap- pinger-Hudson River series of the north side of the Highlands. The writer has elsewhere shown? that the evidence and arguments are not all on one side and that considerable doubt may still be entertained on that point. There is no object in following that argument here or in modifying the treatment here followed of mak- ing them a distinct series. Even if they should prove to be the exact equivalents of the Hudson River-Wappinger-Poughquag series the formations are physically so different and require so different treatment in discussion that they must for our present purpose be regarded as an essentially distinct series. From that standpoint alone the usage here followed is justified. The Man- hattan schist of Westchester county as a type differs as much petrographically from the Hudson River formation of the New- burgh district as the Catskill formation of Slide mountain differs from the Jameco gravels of Long Island. In a discussion where physical or petrographic character is in control there is no doubt about the advisability of treating the two separately. (1) Manhattan schist.2 This is primarily a recrystallized sedi- ment of silicious type. It occurs as a nearly black or streaked, micaceous, coarsely crystalline, strongly foliated rock. The chief constituents are biotite, muscovite and quartz. Quartz, feldspar, 1Dana, J. D. On the Geological Relations of the Limestone belts of Westchester county, N. Y. Am. Jour. Sci. 20:21-32, 194-220, 359-75, 450-56 (1880) ; 21 :425-43; 22:103-I9, 313-15, 327-35 (1881). 2 Berkey, Charles P. “Structural and Stratigraphic Features of the Basal Gneisses of the Highlands.’ N. Y. State Mus. Bul. 107 (1907), p. 361-78. 3 Manhattan schist of Merrill. N. Y. State Mus. 50th An. Rep’t, 1:287. Same as “ Hudson schist,” of N. Y. city folio no. 83. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 49 garnet, fibrolite and epidote also occur in large quantity. Occa- sional streaks or masses are hornblendic instead of micaceous. These are interpreted as igneous injections. They are especially abundant on Croton lake and near White Plains. It is essentially a quartz-mica schist. But it is almost everywhere very coarse textured and hardly ever exhibits the fine grained, uni- form structure of typical schist. Its abnormal make-up — the pre- dominance of biotite and quartz —is the best defense for its petro- graphic classification. The abundance of mica makes it a tough rock but not very hard. The joints and fractures formed in later move- ments are not healed and zones of bad shattering are susceptible to considerable decay. These crushings are sufficiently common to en- courage borings to tap their content of water for small family use throughout Westchester county; but they do not represent large circulation in any case. On the whole, the rock if fresh is good and durable. It may, though rarely, carry considerable sulphide. Practically all of the strictly original sedimentation marks are de- stroyed by metamorphism. The formation has great thickness, but because of the destruction of original bedding lines by recrystalli- zation and additional complication by most complex folding, shear- ing, crushing and faulting, the structure can not fully be unraveled and the thickness can not be estimated with any approach to ac- curacy of detail. But there is probably a thickness represented of several thousand feet. (2) Inwood limestone or dolomite. This formation lies beneath the Manhattan. It is everywhere coarsely crystalline either massive or strongly bedded, often very impure with development of second- ary (recrystallized) mica (phlogopite) and other silicates, espe- cially tremolite. It is essentially a magnesian limestone or dolomite in composition. There is an occasional quartzose bed in the midst of the limestone as at East View. The upper beds are most charged with mica and occasionally beds attacked by alteration have much green, flaky chlorite. There are occasional interbeddings of lime- stone and schist as a transition facies. The coarser grades upon exposure to weathering readily vield by disintegration to a lime (calcite) sand resembling rouchlv an ordi- nary sand in general appearance. At Inwood, the type locality, this disintegration is so pronounced that great quantities are readily shoveled up and used for various structural purposes in the place of other sand. This dolomite is especially liable, as now shown by extensive explorations, to serious decay to great depth. The under- ground circulation seems to attack the micaceous beds with great 50 NEW YORK STATE MUSEUM success and in some places the residue after this solvent action is of the consistency of mud. A nearly vertical attitude of the beds accentuates the opportunity. The most troublesome piece of ground encountered on the whole line of the New Croton aqueduct, con- structed in 1885, was in a weak zone and crevice in the Inwood near the village of Woodland on the margin of the Sawmill valley [see discussions of Bryn Mawr siphon and New York city distributions in part 2]. The thickness probably varies but in many places where there is only a narrow limestone belt it is due more to shearing or faulting out than to original thinning. The most satisfactory estimates are based on the explorations at Kensico dam and the field observations at 152d street. They indicate an approximate thickness of 700 feet. But in all cases either the margins are obscured or there is possibility of faulting to modify measurements. There are no fossils. Weath- ering and erosion has almost everywhere developed valleys or de- pressions especially small tributary valleys in all formations, but as pointed out years ago by Professor Dana the principal valleys pre- vailingly coincide with the limestone belts. (3) Lowerre quartzite. At Hastings-on-Hudson and again near Croton lake, there is a quartzite that appears to be conformable with the Inwood above. There is possibly more than 50 feet. It is a simple, clean quartzite. The other quartzites of Westchester and New York county have a more distinct relation- ship to the underlying gneisses with which they are conformable. The Lowerre of the type locality is of this second class. In the great majority of places where this bed would be expected to occur there is not a trace of it. h Older metamorphic crystallines (Grenville series).' “ The lowest and oldest, as well as the most complex in structure and rock variety, of all the formations of the Highlands region of south- eastern New York is essentially a series of gneisses.” Cutting these gneisses as intrusions of various forms are a great number and variety of more or less distinctly igneous types. In form they vary from small dikes or stringers to great batholithic masses ; in 1This interpretation of the larger relations of the complex gneisses constituting the basis of the series, lying below the Manhattan-Inwood- Lowerre series, was presented by the writer under the title: Structural and Stratigraphic Features of the Basal Gneisses of the Highlands. N. Y. State Mus. Bul. 107 (1907). p. 361-78. The accompanying description is largely an abstract of this paper. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 5I the Cortlandt-series to the very acid granites of Storm King moun- tain or the granophyric pegmatites of North White Plains; and in relative age they likewise vary from a period antedating the chief early metamorphic transformation of the Grenville to Postman- hattan time. But these clearly igneous types attain a considerable prominence as separable units in the practical consideration of the problems of the project and on that account the chief ones will be more fully described under the next group. The older portion — the varicus schists, banded gneisses, quartz- ites, quartzose gneisses, graphitic schists, and serpentinous and tremolitic limestone, forming the complex through which and into which the igneous masses have been injected — form together an interbedded series that was originally a sedimentary group. There is nothing known that is older in this region. Its characteristics and relations mark it as in all probability the equivalent of the “ Gren- ville” of the Adirondacks and Canada. No single type and no single characteristic can be given as a simple guide to the identification of this formation. The prevalence of certain varieties or groups of these and the strongly banded structure give a certain degree of character that forms a reason- able working base. The formation includes banded granitic, horn- blendic, micaceous and quartzose gneisses; mica, hornblende, chlorite, quartz and epidote schists; garnetiferous, pyritiferous, graphitic, pyroxenic, tremolitic, and magnetitic schists and gneisses ; crystalline, tremolitic, and serpentinous limestones, aphi-dolomites, serpentines and quartzites; pyrite, pyrohitite and magnetite de- posits. This is the basal series. But it is complicated by a multi- tude of bands of granitic and dioritic gneisses that represent injections of igneous material at a time sufficiently remote to be subjected to most of the early metamorphic modifications. The equally abundant occurrences of quartz stringers and pegmatite lenses though of later origin can nct be separated from this com- plex mass and the whole must be regarded as a physical unit. The occurrence of interbedded limestones and quartzites together with a variety of conformable schists and banded rocks, marks the formation as essentially an old recrystallized sediment. No member of this older unit of the basal complex is sufficiently prominent to indicate a great break or change up to the time of the first great dynamic movements and igneous outbreaks. The following comparatively constant members are sometimes persistent enough to be considered formational units, but even more commonly 52 NEW YORK STATE MUSEUM are obscure as to boundaries or are of too small development to map separately. (4) Interbedded quartzite. Always a quartzite schist and always exhibiting conformity with the banded gneisses and schists. This is regarded as the uppermost member. (5) Fordham gneiss (Banded gneiss). Granitic and quartzose black and white banded gneisses and schists of very complex com- position and structure. (6) Interbedded limestones. Crystalline. Interbedded, very impure, serpentinous and tremolitic, granular dolomites, usually 2 to 50 feet thick, possibly reaching a thickness of more than 100 feet in a few cases. (7) Older intrusive gneisses. Variable types, mostly granites or diorites, strongly foliated sills. Many are of very obscure relations. The line of close distinction between recrystallized sediment, segregations accompanying that change, and true igneous injection can not be drawn. 1 Special additional igneous types. Under this teenie are included the massive or little modified, not at all or only moderately foliated, igneous masses of later origin and local rather than re- gional development. In some cases, however, they are of decidedly controlling importance in the local geology and rise to the status of definite formations. The most noteworthy of these within reach of the aqueduct explorations are: (8) The Storm King Mountain gneissoid granite (9) The Cat Hill gneissoid granite (central Highlands) (10) The Cortlandt series of gabbro-diorites (near Peekskill) (11)9 The Peekskill sranite (east of | Peeksiall) (12) The Ravenswood granodiorite (Long Island City) (13) The pegmatite dikes and lenses (segregational aqueo- igneous type) (8) The Storm King gneissoid granite is one of the largest of the clearly igneous and less completely foliated types. It constt- tutes the whole of Storm King mountain and the larger part of Crows Nest on the west side of the Hudson, and, crossing the river, forms the chief rock of Bull hill and Breakneck ridge. It is a rather acid, coarse grained, reddish granite with considerable gneissoid structure in a large way [sce Hudson river crossings, pt 2]. ! (9) The Cat Hill gneissoid granite is not essentially different from the Storm King type as a physical unit. Its occurrence at a (Ajddng 19}7eAA Jo pseog Aq ydeis0}0 : GO 9UO O} SuIsuOjoq < rH) : oT Nh Ho Teen EEO Ree J } fouo]od O}TUvIG poyulof A[peq & SI YOI oY] “UOISTAIp [[LySyo0g oY} UO JOUUN} UOSTIIvrL) OF [v}10d Ree, GEGLOGY (OF THE NEW “YORK CIty) AQUEDUCT 53 different point (Cat hill), widely separated by other types from the Storm King locality, and in rather large development, is worthy of separate note. It is cut, of course, in the long tunne! through Cat hill. (10) The Cortlandt series of gabbro-diorites occupies an area of about 20 square miles between Peekskill and the Croton river, nearly all on the east side of the Hudson. It includes a very com- plete range of coarse grained, massive, igneous rocks from soda granites, grano-diorites and quartz-diorites to true diorites, norites, gabbros, pyroxenites, and peridotites. They doubtless represent stages or portions in the differentiation of a magma. The inter- relations are only partially determinable, and the petrographic dis- tinctions in detail are not useful here. The area occupied by the Cortlandt series has an uneven hilly surface with no structural trend, and makes the most striking contrast to the ridge and longi- tudinal valley structure of the rest of the region of the crystallines. (11) The Peekskill gramte, a white, or pink massive, very coarse grained, soda granite, occupying approximately 4 square miles 1m- mediately north of the Cortlandt area 2 miles east of Peekskill, is believed to be genetically related to the Cortlandt series. The evidence in favor of such a relationship has been gathered in the prosecution of this work and has not been published. But it may be said that the textures, structure, age, relationship to older crys- tallines, interrelations with the Cortlandt series, consanguinity of mineralogy, and composition all point toward the above relation- ship. In essential relations, therefore, it is the acid extreme of the Cortlandt series. Its economic features, however, are of sufficient importance and its easy differentiation from the regular Cortlandt types require that it should have separate treatment. (12) The Rravenswood grano-diorite occurs chiefly in Brooklyn. It is a slightly foliated mass intrusive in the Fordham gneiss and is doubtless connected in origin with the sources of many of the hornblendic intrusive bands in the Fordham and Manhattan forma- tions in the district. It covers a known area of about 5 or 6 square miles and may be more extensive. The rock is suitable for struc- tural material and has required consideration in the study of “ Dis- tributary conduits ” [see pt 2 East River section]. (13) Pegmatites. The pegmatites and pegmatitic granophyric masses of all kinds are of almost universal distribution in the foliated crystallines. They vary from quartz bunches or stringers to pegmatitic lenses and irregular masses, and to definite granitic 54 NEW YORK STATE MUSEUM or pegmatic dikes. In many places they constitute a large propor- tion of the formation in which they occur. They doubtless vary in age, but for the most part seem to belong to the later period of _metamorphism. Many of them are massive and largely free from foliation. They no doubt have a complex origin between simple aqueous segregation on the one side and true igneous intrusion on the other. Summary of formations Group a Quaternary deposits (1) Glacial drift Occurs as a_ surface Till and modified drift, extra mantle over nearly all marginal outwash, sands and of the region under gravels, etc. discussion, except the immediate sea margin UNCON FORMITY Group b Tertiary and Cretaceous deposits (2) Tertiary outliers (a) Pliocene littoral deposits (Bridgetons?) C es . onfined to Long Is- 2 eciie Buy eae eae land, Staten Island i and the New Jersey (3) Upper Cretaceous beds are (a) Lignitiferous sand (marl series) (b) Matawan beds (clay ae (c) Raritan (clays and sands) UNCONFORMITY Group c Jura-Trias formations (4) Palisade diabase intrusion Confined to the west (5) Newark series of conglomerates, side of the Hudson sandstones and shales south of the High- lands GEOLOGY OF THE NEW YORK CITY AQUEDUCT UNCON FORMITY 56 Group d Devome strata (6) Catskill, white and red conglom- erate (1725 feet) (7) Oneonta (upper flagstone) (3000 feet) (8) Ithaca and Sherburne (lower flag- stone) (500 feet) (9) Hamilton and Marcellus shales (flagstone and shales) (700 feet) (10) Onondaga limestone (200 feet) (11) Esopus and Schoharie — shales (silicious) (800 feet) (12) Oriskany and Port Ewen transi- tion (100 feet) (13) Port Ewen limestone and shale (150 feet) (14) Becraft limestone (75 feet) (15) New Scotland shaly limestone (100 feet) (16) Coeymans cherty limestone (75 feet) | Confined to the Cats- kills, the Esopus and Rondout valleys, the northern extension of the Shawangunk range, and Skunne- munk mountain near Cornwall Group e Siluric strata (17) Manlius limestone (70 feet) (18) Cobleskill limestone and cement beds (30 feet) (19) Binnewater sandstone (50 feet) (20) High Falls shale, including small limestone beds (75-80 feet) (21) Shawangunk conglomerate (250- 350 feet) : Confined to the Rondout and Esopus valleys and the northerly ex- tension of the Shaw- ano wmk) ran se, through the cement region of Rosendale, Binnewater, Rondout and Kingston, and a small outlier at Skun- nemunk mountain 56 NEW YORK STATE MUSEUM UNCONFORMITY Group f ‘Cambro-Ordovicic formations (22) Hudson River slates, shales, and. Especially prominent as sandstones (very thick) (Or- dovicic) more than 2000 feet (23) Wappinger limestone (1000 feet) (in. part ‘Cambric and injipart Ordovicic) (24) Poughquag quartzite (600 feet) (1) The Manhattan (Cambric) surface formations in the Shawangunk range, the Wallkill valley, and the region eastward and_ south- ward to the High- lands, on both sides of the Hudson Group g Later crystallines (South of the Highlands) (Uncertain age) schist, a thor- oughly and coarsely crystalline sediment of uncertain age — generally supposed to be equiva- lent to the Hudson River slates, (Ordovicic) but here separated without necessarily raising that question because of their very different physical and _ petro- graphic character (2) Inwood limestone (or dolomite), a magnesian crystalline lime- stone of uncertain age, generally supposed to be the equivalent of the Wappinger (Cambro-Ordo- vicic), but here enumerated sep- arately without necessarily rais- ing that question because of their very different lithologic character and associates (3) Lowerre quartzite, an occasional quartzite of uncertain relations and very limited development ] | | | | | | | | | | | | | Confined to the region east of the Hudson river and * sottht "or the Highlands proper, occupying the region from the Highlands to Long Island GEOLOGY OF THE NEW YORK CITY AQUEDUCT 57 UNCONFORMITY Group h Older crystallines (Highlands gneisses) (Grenville series of metamorphics and intrusives — Precambric) (4) Interbedded quartzite. A Formations © character- quartzose schist istic of the High- (5) Fordham gneiss (chiefly lands and some of sedimentary). Granitic larger ridges extend- and quartzose banded ing southward to gneisses and schists of ener Neways Mot icity A very complex develop- we series, which in petro- ment Bene graphic variety, is as (6) Interbedded limestones | complex as all of the (Grenville) associated | rest of the forma- with the Fordham | tions of the region gneisses together vo Old intrusions. Large and varia- | ble masses of granitic gneisses of igneous origin cutting the Grenville series, such as Storm King granite, Cat Hull granite, Che: ! | Postgrenville in age Group 1 Special additional igneous types (8) Storm King gneissoid granite, These are masses of Storm King-Breakneck district strictly igneous origin (9) Cat Hill gneissoid granite. Garri- (except the pegma- son district tite) > cand, vot Glarger (10) Cortlandt series of gabbro-diorites. development = which Peekskill-Croton district citer yy becatise yy (01 (11) Peekskill granite. A boss, related their abundance (peg- to the Cortlandt series. Peeks- matites) or large area kill district (Cortlandt) or eco- (12) Ravenswood _ grano-diorite. A MO WiC yy ireare Ww hie’s boss. Brooklyn, Long Island (Peekskill) or im- City and Southern Manhattan portant bearing upon (13) Pegmatites. Dikes, lenses, segre- the plans of the aque- gations of general distribution duct (Storm King) are worthy of sepa- rate note. 58 NEW YORK STATE MUSEUM 3 Major structural features In addition to the simpler structural characters of the strata, already sufficiently emphasized in the individual descriptions, there are numerous others of more general relation whose value and in- fluence it is necessary to consider in many of the practical problems. Those of most importance are the unconformities, folds and faults. They are directly related to continental elevation and subsidence, to mountain forming movements and denudation processes, to meta- morphism and to igneous intrusion. a Sedimentation structures. In the younger strata the prin- cipal structures are those of bedding, stratification, conformable succession, etc., characteristic of all sediments of such variety of type. These are prominent in the older groups of formations down to the crystallines, but the earlier Paleozoics are also affected so profoundly by folding and faulting that attention is more concerned with these induced or secondary structures. b Unconformities. Time breaks, with more or less disturb- ance of strata and accompanied by erosion, are numerous. (1) That between the glacial drift and the rock floor is the most profound. It causes the glacial drift to lie in contact with every formation of the region from the oldest gneisses of the Grenville series of the Highlands to the traces of Miocene beds of Long Island: (2) The interval between the Pliocene and the Upper Creta- ceous beds is more obscure and hardly reaches the importance of an unconformity. It is probably more nearly of the value of a disconformity or of an overlap, and the very limited development of the overlying beds in the region gives little chance for determin- ing relations in much detail. (3) The overlap and unconformity between the Cretaceous and Triassic. A condition determinable only on the New Jersey side of the Hudson river. (4) The unconformity between the Triassic and underlying formations of different ages. An interval representing mountain development and extensive erosion, in which the chief movement probably belongs to the close of Paleozoic time and includes the Appalachian folding. (5) Unconformity between Siluric and the Ordovicic strata. An interval representing mountain development, folding and erosion, in which the movement known as the Green Mountain folding took place. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 59 (6) Unconformity between the Poughquag (Cambric) quartzite and the underlying crystallines. An interval-in all observable cases of great length and profound changes involving mountain folding, metamorphism of the profoundest sort, and extensive erosion. (7) Among the crystallines of the south side of the Highlands there is one break of similar importance, between the Inwood lime- stone and the underlying gneisses. Whether or not it is the same as no. 7 above is not clear, but even if it represents the same break the relations are somewhat different in degree and character because of the lack of quartzite in almost all cases. Within the gneisses of the Grenville series and their associates of all kinds there are no breaks of the unconformity type known. The contacts are eruptive in character, or are displacements instead. c Folds and mountain-forming movements. All of the forma- tions from the oldest up to and including the Lower Devonic strata are folded. Many of the smaller (minor) folds exhibit complete form in the stream gorges of the district, but all of the larger ones, the main folds, have in earlier time been eroded to such extent that the series is beveled off and only the truncated edges are to be seen, exhibiting strata standing more or less perfectly on edge, and making restoration of the form a very difficult or impossible task. This is only partially accomplished in the Siluro-Devonic margin along the Shawangunk range; it is more complete in the Cambro-Ordovicic north of the Highlands, and it reaches its most perfect development in the crystallines of the Highlands and New York and Westchester counties. These differences correspond roughly to the differences in age of the strata, and, taken together with the evidence of the profound unconformities, indicate that mountain-forming movements of far-reaching importance visited the region no less than three times. Each time of such disturbance, of course, the underlying older series was affected by the move- ments of that epoch in addition to any previous ones, and as a con- sequence the older is to be expected to show more complexity of such structures. Each succeeding series separated by such activity is therefore one degree simpler in structure. | Of these three epochs of great disturbance, one is (1) Precambric and corresponds to the time interval marked by the unconformity between the Poughquag quartzite and the gneisses: a second (2) is Postordovicic and corresponds to the time interval marked by the unconformity between the Hudson River slates and the Shawan- 60 NEW YORK STATE MUSEUM gunk conglomerates, and the last (3) is Postdevonic (probably Postcarbonic, judging from neighboring regions of similar history) and has left as its most important evidence in this district, the excessively complicated sharp foldings and thrusts of the Shawan- gunk range and its extension in the Rosendale cement district. Kinds. As to forms produced there are no usually described types that are not to be found here. The simpler forms of anti- clines and synclines, both open and closed, symmetrical and unsym- metrical and overturned, are all common. The isoclinal is common in the gneisses. In each epoch of folding the compression forces were effective chiefly in a northwest-southeast direction producing arches and troughs whose axes trend northeast-southwest. This is the trend of the main structures throughout the region. The extent of crustal shortening accomplished by this series of compressions is undetermined, but that it -amounts to a total of many miles is indicated by the fact that over broad areas the strata stand almost on edge. Furthermore, in the older Highlands and in portions of the Hudson river districts the folds have been slightly overturned so that commonly the strata on both limbs dip in the same direction (toward the southeast). This seems to indi- cate a strong thrust from the southeast. All stages between the gentlest warping to strongly overturned folds, and from minute crumbling to folds of great extent and persistence are to be seen. The effect of all the folding is chiefly to present a series of up- turned strata to erosion and encourage a subsequent development of valleys along the softer beds bordered by ridges of the more resistant types. As the axes of the folds lie in a northeast-southwest direction, this gives a marked physiographic development of ridges and val- leys of the same trend, a most conspicuous topographic feature of southeastern New York. d Faults. Accompanying the folding in each epoch, and especially the stronger overthrust movements there has been a tendency to rupture and displacement. These breaks are known as faults. Multitudes of them are of minute prcportions and prac- tically neglectable in a broad view, but many also are of large extent, traceable across country for many miles and indicating dis- placements in some cases of many hundreds of feet. For the most part these faults are of the thrust type and wholly consistent with the folds in origin. They run generally in a northeast-southwest direction, especially the larger ones, and frequently form the sep- aration planes between different formations. Occasional cross (3061 ‘Asojoarn ur [ooyss Jstuwns B]IO9S MON 24} Ur ploy y AVISIOAIUAY vIquInjod Aq ydersojoyq) “49219 jnopuoy uo su SOW] pu OI 91eIq (8061 ‘ASOTO95) ul [OOYSS sJewuINS AjIstoAIUG Biquinjo Aq ydersojoyd) ‘o[epussoy Ivou YaeI9 jnopuoY uo speq ouojsouy 9y} ut yney isniyi V II 9}®[q ‘ GEOLOGY OF THE NEW YORK CITY AQUEDUCT 61 faults occur (with northwest-southeast direction across the strike), but so far as is known they are always of minor consequence. In rare instances, the trace of a fault-line on the surface describes curious curves, such as that at Cronomer hill above Newburgh, apparently inconsistent with the chief structural trend, but a study of the whole geologic relation in such cases shows them to be con- nected with the projecting spurs of underlying formations which in any large thrust movement plow their way with some success through the younger overlying, less resistant, strata. They differ in no material way from the cther more simple !ooking lines. Both normal and thrust faults occur, but the thrust type appears to be most common. The amount of displacement cr throw is extremely variable. The larger faults represent movements of several hundred feet. In rare cases the movement may be as much as 2000 feet. The effects may be grouped as follows: (1) the appearance of formations out of their normal order, i. e. contacts between forma- tions that do not normally lie next to each other; (2) the produc- tion of escarpments, 1. e. steep cliff-bordered ridges; (3) the de- velopment of zones of more or less extensively crushed rock along the principal plane of movement; (4) the determination of loca- tion for stream courses and gulches and valleys that cross the formations. All of these effects are more noticeable and better preserved for the later movements than for the earlier ones. Many of those dating back to the earliest epoch, affecting only the crystalline rocks of the Highlands, are not readily detected. Most of the breaks have been healed by recrystallization and the contacts are often as close and sound as any other part of the formation. But this is not so true of the later epochs — and in them a good deal depends upon the type of rock affected. The more brittle and hard and insoluble types are more likely to still have open seams and unhealed fractures than the softer and more easily molded formations. In some of these, recent water circulation has still further injured the fault zones by introducing rock decay to con- siderable depth. Because of the more ready circulation in them, it is noticeable that some of the extensive decay effects are produced in crystalline rocks that otherwise very successfully resist destruc- tion. On the whole the softer clay shales and slates are less likely to preserve open water channels of this sort than any other forma- tion of the region. 62 NEW YORK STATE MUSEUM No part of the region is wholly free from faulting effects, except perhaps a part of Long Island. The Catskills also are very little affected — so little that this type of structure has not require con- sideration in the vicinity of Ashokan reservoir. But all parts of both the northern and southern aqueduct system have had this feature to consider. Further discussion of the specific local problems introduced by faulting and folding is given under the problems of part 2. A con- siderably more extended comment on the age of fault movement is given under the heading “ Postglacial faulting.” 4 Outline of geologic history Most of the general features of geologic history have been involved more or less in the foregoing discussion. It is im- -possible to wholly separate matters that are so intimately inter- related even though it 1s convenient to think of or consider one phase at a time. But it may serve a useful purpose to summarize the steps of progress as illustrated by local geology from the earliest geologic time to the present. a Earliest time. (Prepaleozoic, Agnotozoic, Proterozoic, or Azoic Era). There is little doubt that the oldest rocks known in this region are representatives of a time of regular sedimentation. Conditions favored the deposition of silicious detritus of variable composition with an occasional deposition of lime, nearly always in very thin beds. What these sediments were laid down upon or where they came from are unsolved questions. The remnants of them that are still preserved are the basis of the “ Grenville series ”’ as interpreted in this area, and are the basal (oldest) members of the “ Fordham” or “ Highlands gneisses.” How long ago this series was deposited is not known. It can be stated only approximately even in the rather flexible terms used in historical geology. It is older than any Paleozoic strata (Pre- cambric), probably very much older. It is even possible that this series is as much older than the Cambric as that period is compared to the present. In short, it is not known, and there is apparently little immediate likelihood of finding out even to which of the sev- eral subdivisions of the Prepaleozoic this series belongs. It is cer- tain that before the Cambric sandstones of the Paleozoic era had begun to form, this older series was disturbed by crustal move- ments, folded, metamorphosed, intruded by igneous injections, ele- vated above the water (sea) level of that time and eroded by sur- face agencies. These movements and steps there is no doubt of. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 63 When subsidence! again depressed the area beneath the sea the deposition of sands that we now call Cambric (Poughquag) quartz- ite began. | b Early Paleozoic time. With the sedimentation upon this old crystalline rock floor a long time of apparently continuous deposi- tion began which ultimately resulted in the accumulation of several thousand feet of sandstones, limestones, and sandy or clayey shales that are now known as the Cambro-Ordovicic series (Poughquag- Wappinger-Hudson River series). But at the close of Ordovicic time or late in that period another crustal revolution began. The whole region was again compressed into mountain folds, faulted, sheared, metamorphosed, elevated above sea level, and subjected to erosion. This corresponds to the Green mountains folding of Vermont. With the next subsidence and a return of sedimentation a new series began to form. The break marking the occurrence of all these changes, known locally as the Postordovicic unconformity, represents a considerable portion of Siluric time. c Middle Paleozoic time. ‘The earliest deposits of this series, which continued to accumulate through late Siluric and all of De- vonic time, were heavy conglomerates very unevenly distributed over the new rock floor. “These are the so called Shawangunk con- glomerates, a formation that within the boundaries of this imme- diate area and within a distance of 20 miles varies from a thickness cf more than 300 feet to almost nothing. But for the most part, sedimentation was regular and fairly continuous and of immense volume. The whole series of conglomerates, sandstones, shales, grits and limestones belonging to the later Siluric and the Devonic are included. Not all are believed to be marine however. The Catskill and Shawangunk conglomerates may well be of continental type. Long after the deposition of all of these strata another crustal disturbance, for at least the third time, repeated the process of mountain-folding and erosion. This was the time of the Appalach- ian mountain-folding. In this region it caused a wonderfully com- plex development of folds and faults that are especially important and determinable as to type and age in the Rondout cement region. The movement, of course, affected all of the older formations as 1 There may possibly be an intermediate stage, practically a duplication of the whole as given above, between the very oldest and the Cambric, represented in the “later crystallines,” but this may as well be neglected for the present. 64 NEW YORK STATE MUSEUM well, but on them, already disturbed by earlier displacements, the features chargeable to the disturbance can not always be distin- guished from older ones. All three of the mountain-forming com- pressions seem to have been controlled by the same relationship of forces and adjustments of movement, for the results are in each case the production of folds or faults of similar orientation and a final structure of uniform trend. Deposition had been going on for ages, chiefly on the west and north side of the older crystallines ; but with a return of sedimenta- tion a decided reversal is noted. The Atlantic border is depressed and much of the interior region seems not to have been subjected to further deposition from that time even to the present. d Mesozoic time. Again conglomerates, sandstones and shales were laid down upon an eroded floor. From their condition and lithology it is believed that they are partly of continental, flood plain, origin. The series is thick, generally assigned to the Triassic period and is extensively developed. During the time of accumula- tion and to some extent subsequent to it, there was extensive igneous activity pouring out and intruding basic basaltic matter in large amount. The Palisade diabase sill, and the Watchung Moun- tain basalt flows are the best examples. At a later time small faulting occurred making frequent dis- placements in this series. But mountain-folding has not again visited the region. Such breaks as there are, are of the nature of overlaps and disconformities rather than of the revolutionary his- tory indicated by a true unconformity. One of these intervals occurs in the Mesozoic between the Triassic and Cretaceous. Above it the thick series of Cretaceous shales, marls, sands and clays are developed. Succeeding this series a similar interval represents the earliest Cenozoic time. c Early Cenozoic time. The earliest Cenozoic (Eocene and Oligocene) has no sedimentary record within this region. There are small remnants of deposition representing Miocene and Pliocene time. Above these again the record is blank up to the time of the glacial invasion. f Late Cenozoic time — glacial period. By some combina- tion of conditions not very well understood, the chief features of which no doubt are,—(1) continental elevation and (2) shifting of centers of precipitation and (3) modification in the composition of the atmosphere, a period of excessive ice accumulation was inaugurated. Ice finally covered immense continental areas and GEOLOGY OF THE NEW YORK CITY AQUEDUCT 65 from its own weight by continuous accumulation spread out (flowed) from great central areas toward the margins. There is clear evidence of interruptions or advances and retreats of this general movement many times. But the same type of work and similar results were attained in each case. The chief features of this work was the moving of rock material frozen in the ice to long distances and the deposition of it again, more or less modified by its contact with the ice or by the effect of water upon its release, at other places and with entirely new associations. The tendency to ice accumulation was finally overcome to sufficient extent for the inauguration of the present condition of things. Whether it is a permanent change or only an interglacial interval is not clear. But the ice has withdrawn to the mountains and the polar north at the present time. It has not occupied the surface of this region probably within the last 40,000 years, and perhaps for a much longer time. 5 Outline of geographic history — physiography The surface features of a country are the result of the working out of a long and complex series of processes with and upon the materials of the rock floor or bed rock. The relationship of surface features to the formations that occur in the rock floor and their stages of development, in short, an interpretation of their origin and meaning, constitutes geographic history or physiography. — It differs little in essential character from geologic history, of which it is only a special branch, i. e. the history of surface configuration. And it can not be appreciated or understood except in the light of a thorough knowledge of stratigraphic and structural geology. In individual cases or particular regions the geologic knowledge must also he specific. a Early stages. Occasional glimpses of surface features, and some scattered facts about their development are to be gathered of older continental existence. Surface features characteristic of their time were developed in the great intervals between each successive period of continuous deposition. Traces of them are involved in the unconformities of the geologic column already shown in the discus- sion of geologic history. Hills, valleys, streams, shores and all the appropriate assortment of forms must have existed. But they could not have been like those of the present in many minor fea- tures — especially in arrangement and distribution— because the bed rock of those times had only in part reached the complexity of 66 NEW YORK STATE MUSEUM structure and composition now belonging to it. Many items of im- portance are indicated in some of these early periods. For ex- ample, the sea encroached on the land borders repeatedly from the westward — especially throughout Palezoic times, while in Meso- zoic and Cenozoic times the evidence of shiftings of sea margins is confined to the east and southeast borders, and likewise probably no near by place has been continuously beneath the sea. But the unraveling of these conditions is obscured by subsequent events. Land surfaces that once were, became covered by later sediments. The physiography of those times, Paleophysiography, as well as paleogeography, is therefore a difficult and intricate line of investigation. With these ancient surfaces the dicussion of present features has little to do. Here and there the present surface cuts across and exposes the edges of an older one giving traces of the old profile; but in most cases it is so distorted by the foldings and other displacements belonging to a later period that a restoration of the original continental features is a task fit for the most highly trained specialist. The surface as it now exists, and the rock floor modified only by the inequalities of the loose soil mantle, yields more readily to in- vestigations of origin and history. | b History of present surface configuration. On some por- tions of the region there seems to have been no deposition since the close of Paleozoic time. Throughout most of Mesozoic and Ceno- zoic times, therefore, those regions probably have been continuously land areas (continental) and have been subjected to the agencies of erosion. This applies particularly to the Highlands region and the Catskills and the Shawangunk range and intervening country. What the surface configuration was like in the early stages is wholly unknown. In the beginning, mountain-folding — the Appa- lachian folding — was in progress and the features were probably those of partially dissected anticlinal folds. With the progress of erosion the Triassic deposits were accumulated along the eastern border, probably on the continental slopes. Subsequently, further elevation extended erosion over the Triassic areas also and the Cretaceous beds were laid down on the margin. The general lines of development have been the same from that time to the present. Each successive important formation less heavily developed and forming a band outside of and upon the older one — the whole now constituting a series of successive belts the oldest of which is far inland and the newest at the sea margin. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 67 Therefore, when long periods of denudation are referred to, it is well to appreciate that this is especially applicable to the interior, that the sea margins are comparatively new, and that certain of the inland areas were suffering erosion long before the rock forma- tions that lie beneath and form the rock floor of the sea border districts were in existence. Cretaceous peneplain. It appears from studies of these problems in a broad way, and, drawing upon generalizations from continental features of a much larger field than that of the present study, that the continental region of which this forms a part must, in the earlier periods, have remained in comparatively stable equilibrium for an extraordinarily long time. So long a time elapsed that most of the area was reduced by erosion to a monotonous plain (pene- plain) at a very low altitude, probably not much above the sea (base level). Only here and there were there areas resistant enough or remote enough to withstand the denuding forces and stand out upon the general plain as remnants of mountain groups (Monad- nocks). Possibly the Catskill mountains of that day had such relation. This reduction of surface feature it is believed was reached in late Cretaceous time. The continent stood much lower than now. Portions that are now mountain tops and the crests of ridges were then constituent parts of the rock floor of the peneplain not much above sea level. This rock floor was probably thickly covered with alluvial deposits (flood plain) not very different in character from the alluvial matter of portions of the lower Mississippi valley of today. Upon such a surface the principal rivers of that time flowed, sluggishly meandering over alluvial sands and taking their courses toward the sea (the Atlantic) in large part free from influence by the underlying rock structure. The ridges and valleys, the hills, mountains and gorges of the present were not in existence, except potentially in the hidden differences of hardness or rock structure. Such conditions prevailed over a very large region — certainly all of the eastern portion of the United States. This so called ‘Creta- ceous peneplain is the starting point in development of the geo- graphic features of the present. Continental elevation. Following upon this period of stability and extensive denudation came one of continental elevation. How much above sea level this raised the areas under present discussion may not be determined, but that it was a sufficient amount to 3 68 NEW YORK STATE MUSEUM rejuvenate the streams and permit them to begin the sculpturing of the land in a new cycle of erosion is perfectly clear. As soon as the elevation and warping of the continental border made its influence felt in the increased activity and efficiency of the streams (rejuvenation) they began transporting the alluvium of their flood plains and to sink their courses through this loose material to bed rock. ‘The final result of long continued denudation under these conditions in early Tertiary time was the removal of the loose mantle and the beginning of attack on bed rock (superimposed drainage). The streams formerly flowing on alluvium that had now cut down to rock found themselves superimposed upon a rock structure not at all consistent with their former courses. With the progress of erosion on this rock floor all these differ- ences of structure, such as the differences in hardness of beds, the trend of the folds, the strike of the faults, the igneous masses, etc., were discovered and the streams began to adjust their courses to them. Valleys were carved out where belts of softer rock occur, ridges were left as residuary remnants where belts of harder rock exist, and the surface (relief) took on some of the char- acter of present day lines. That is, the principal mountain ranges of that time were the same as those of today in position and trend; but they had not so great apparent hight because the in- tervening valleys had not yet been cut so deep. The principal escarpments of that time were due to the same structural lines as those of today, only they have shifted somewhat along with the general retreat of all prominences by the forces of weathering and erosion. | In the course of this work of sculpturing and the shifting of valleys and divides and escarpments and barriers into constantly greater and greater conformity with rock structure, it came about by and by that practically all of the smaller and tributary streams had so completely adjusted themselves to their geologic environ- ment that their valleys almost ‘everywhere followed along the softer beds (subsequent streams), the divides were chiefly of harder beds, the trend of both were almost everywhere parailel to the strike of the rock folds and other structures (adjusted drainage). This undoubtedly involved in many cases a very radical change of stream course, and in some cases an ultimate reversal of drainage to such extent that tributaries were deflected inland against the course of the master streams and in some cases actually flowed many miles in this reversed direction before finding an accordant junction (retrograde streams). At least three of the streams of ‘ GEOLOGY OF THE NEW YORK CITY AQUEDUCT 69 southeastern New York are still of this type—the Wallkill, the Rondout and the lower portion of the Esopus. But the larger rivers, the great master streams, of the super- imposed drainage system, in some cases were so efficient in the corrasion of their channels that the discovery of discordant struc- tures has not been of sufficient influence to displace them, or re- verse them, or even to shift them very far from their original direct course to the sea. They cut directly across mountain ridges be- cause they flowed over the plain out of which these ridges have been carved and because their own erosive and transporting power have exceeded those of any of their tributaries or their neighbors. They are superimposed streams (not antecedent), they have, with their tributaries, settled down in the ancient plain, and, by their own erosive activity, have carved the valleys deeper and deeper, cutting the upland divides narrower and narrower until now only here and there a ridge or a mountain remnant stands with its crest cr summit almost reaching up to the level of the ancient pene- plain on which the work began. If the transported matter could all be brought back and replaced in these valleys the old plain might be restored, but the work would immediately begin al! over again. Of these great master streams the Hudson is the only local rep- resentative [see Study of the Hudson River gorge in part 2]. Tertiary incomplete peneplanation. Such processes, ii allowed ta continue on a stable continental region. would ultimately reduce the land for a second time to a monotonous plain (complete cycle of erosion). The beginnings of such a plain would be made in the principal stream valleys upon reaching graded condition. Their lateral planation and the development of flat-bottomed valleys would begin at about the level that the plain would stand in the final completed stage. The difference of elevation between the ridge crests or hilltops and these flat valleys, 1. e. between the old peneplain and the new unfinished one would be an approximate measure of the amount of the continental elevation that instituted the new cycle. : But judging from such remnants of this later plain as are to be seen, the two, i. e. the old Cretaceous peneplain and the new Tertiary peneplain are not parallel. Toward the southeast, toward the sea, the oider plain descends more rapidly than the younger and intersects it. Both pass beneath sea level in that direction. The difference between them therefore varies with locality from 7O NEW YORK STATE MUSEUM o feet to perhaps 2000 feet within the borders of the area (con- tinental tilting or warping). Late Tertiary reclevation. Traces of such an intermediate and incomplete peneplain are to be seen in the compound nature of the large valleys of the present day. Most of them are essentially broad valleys into the bottoms of which narrower valleys and gorges are cut. The tops of the minor hills and ridges of the broad valleys represent the intermediate Tertiary peneplain that was interrupted in its development before completion (interrupted erosion cycle). The inner narrow valleys indicate that for the second time a re- gional elevation rejuvenated the streams and they began their work of cutting to a new grade. They have made a good begin- ning at this task, and as a consequence have carved some reliet in the old valley bottoms. These new streams have not yet reached a graded condition. . When the glacial ice began to invade this region all of the surface features had had such a history. Leaving out of account minor fluctuations of elevation and depression, of which there may have been several of too transient character to make a lasting impres- sion on the topography, the stages become comparatively few and the general tendencies are easily understood. The measurable differences of elevation between the Cretaceous and Tertiary peneplains give some reasonable conception of the amount of the first continental or regional elevation. Concerning the altitude reached in subsequent regional elevation there is less certainty. None of the streams, not even the master streams such as the Hudson, reached grade, for it exhibits strictly a gorge type not only within’ the present land borders, but it is now known to show gorge development far beyond the present coast line. Judg- ing from the Hudson, therefore, it seems necessary to conclude that this continental region stood at a much greater elevation in some portions of the later period than had formerly prevailed. Probably the maximum elevation immediately preceded the glacial invasion. Conservative estimates as to the amount of elevation of that time in excess of the present would place it at not less than 2000 feet. Much more than that is believed to be indicated, possibly 5000 feet or more. In the meantime, the master stream, the Hudson and several of the tributaries cut into their valley bottoms to such extent as to make typical gorges so deep that their beds now, since the sub- GEOLOGY OF THE NEW YORK: CITY AQUEDUCT 71 sidence, lie much below sea level. The Hudson bed is of this character throughout its course from Albany to the Atlantic, and in the Highlands, 60 miles inland, the known rock bed at one point is more than 700 feet below sea level. In late glacial time there was still greater subsidence (50-100 feet) than the present as is indicated by terraces above present water level and the deltas formed at the mouths of tributary streams. Such in general outline is the history of successive conditions governing the topographic development of the rock floor. The suc- cession of periods of stability, elevation, stability again, reelevation and subsidence have had an effect on all sorts of formations, but the extent of the impress and its permanence varies greatly in the different districts. It is not possible to study these differences in detail here. They are the minor and special local characters that are in control at particular localities. In discussions of special problems some of these are taken up in more detail. But in each case the general history as outlined above, together with the modi- fying influence of known local structure and stratigraphic char- acter are the foundations of a working understanding [see Hudson River crossings, Moodna creek, Rondout valley, etc., pt 2]. Pleistocene glaciation. An additional modification and one largely independent of and largely inconsistent with the distribution of the smaller features of the rock floor is introduced by the glacial drift. It covers almost everything, but so unevenly as to largely destroy some of the detail. It is in places more than 350 feet thick (as in the Moodna and Rondout valleys) and in others it amounts to nothing. It covers the narrow ravines and gorges heaviest and has altered the courses of many of the smaller streams, the original channels being hopelessly buried. The result has been chiefly one of reducing the ruggedness of outline that prevailed along the newer gorges of late preglacial time. Besides this the usual surface forms characteristic of glacial de- posits, occur — the kame, the drumlin, the esker, the hill and ket- tle topography of the terminal moraine, the overwash plain, the delta, the lake deposit and the gentle undulations of the ground moraine. These are superimposed on the rock floor features. Both are equally important to understand in the problems that have been encountered. Which set of factors is to be most regarded in a given case depends wholly upon the locality and the kind of en- terprise or work it is proposed to undertake. 72 NEW YORK STATE MUSEUM c Physiographic interpretation. Rock floor contour is an ex- pression of the differences in character and structure of the bed rock formations themselves, brought about by ordinary surface weathering and transporting agencies, varied in their action and effects only by certain differences in elevation above the sea. It is apparent therefore that it would be possible by careful observa- tion of surface features to gather data sufficiently definite to fur- nish a basis for suggestions about hidden and hitherto unknown or undiscovered structural and stratigraphic characters. But the application of it to practical engineering problems is a complicated and difficult matter. And this difficulty is nowise simplified by the occurrence of a drift soil that tends to obscure many of the more delicate features. For example, the later narrow stream gorges marking the stage of extreme regional elevation are com- pletely buried. Only an occasional stream like the Hudson has maintained its course unchanged and has begun excavating the channel again. But even in this case, as will be shown under a separate head, the work of reexcavation is only just begun and the amount yet to be done and the corresponding original depth of the gorge are wholly unknown. Certain surface features, however, are readable and, considered with due regard for all possible causal factors, give very useful suggestions. From them one obtains clews as to (1) the attitude or relations of the hard and soft beds and the weak zones, (2) the dip and strike of strata, (3) the persistence of a formation, (4) the occurrence of faults, (5) the direction of the chief dis- turbances, (6) the resistance and durability of local rock types — in short the structural characters of all kinds because differences in the distribution of these characters have given the different topo- graphic forms and geographic areas. They have made the features of the Highlands look different from those of the Catskills, and those of Wallkill valley different from the Croton. Because of the long train of conditions with which these surface features are each involved and the structures that they indicate they become easily the chief factors in preliminary judgment of comparative practicability of rival locations, and are the most reliable guide to direction and character and extent of exploratory investigation for many engineering enterprises. d Physiographic zones. In summarizing the physiographic data it appears that the following belts or zones may be regarded as fairly distinct units: GEOLOGIC FORMATIONS — Catskill and Oneonta sand- stone conglom- erates Sherburne flags Hamilton and Marcellus shales Onondaga lime- stone Esopus grit The Helderberg series Shawangunk conglomerate Hudson River shales, sand- stones and slates Wappinger lime- stone Poughquag quartzite Storm King = --_ “~granite , The Highlands gneisses Plate 12 The Catskill | mountains Ashokan [reservoir Hamilton escarp- ment Esopus creek High Falls Rondout creek Shawangunk mountains Wallkill river Hudson river New Hamburg Wappinger creek Fishkill creek Newburgh Breakneck Mountain Storm King mountain Bull mountain Crows Nest Foundry brook Cold Spring West Point Relief map of the region from the Catskill mountains to the Highlands © showing the principal physiographic features. also the areal and structural geology.) | Ie physiographic laboratory of Columbia University by Messrs Billingsley, Grimes and Baragwanath) (The original model shows (Taken from model made in the GEOLOGY OF THE NEW YORK CITY AQUEDUCT 73 (r) Coastal plain. A district underlain by Cretaceous and later recks and confined to a part of Staten Island and Long Island, not exceeding 400 feet relief. This zone is characterized by den- dritic drainage, except a narrow belt on its inner margin which is a longitudinal valley of the “inner lowland” type. Long Island sound occupies the position of this old adjusted valley. (2) Piedmont belt. A district lying between the coastal plain and the Highlands. It is underlain chiefly by crystalline rocks and metamorphosed sediments. Not exceeding 800 feet relief. It 1s characterized by adjusted drainage obscured only by drift. The ridges and valleys trend northeast and southwest close together and with very little variation on the east side of the Hudson, while on the west side the gentle dips of the Triassic give broader and more unsymmetrical forms with dip slopes and escarpments wholly independent of the opposite side. The zone is essentially transitional between the simple forms of the coastal plain and the complex mountainous character of the Highlands. . (3) Highlands. The rugged elevated zone formed by the crys- talline gneisses. Reaching elevations of 1600 feet. It is character- ized by irregular mountain masses and lofty ridges of a general northeast trend but with many prominent irregularities both: of form and of drainage. The valleys are deep and narrow. There are many steep escarpments. It is a mountainous zone in which complex structures and rocks have led to the development of com- plex forms. The zone forms a sort of barrier 20 miles wide across the Hudson river which exhibits its most zigzag and narrow and gorgelike development in this district. (4) Appalachian folds. Characterized by folded Paleozoic rocks north of the Highlands. Reaching elevations of 1500 feet rarely — general relief 400-800 feet. North of the Highlands the relief is much less pronounced. The softer rocks of the early Paleozoic formations permitted the development of a broad valley with almost perfectly adjusted tributaries, most of which on the west side of the Hudson are reversed. The topographic forms give expression to the universal folding and faulting of the formations. It is essentially a transition from the complex mountain zone of the Highlands to the much simpler Catskill area. (5) Catskill Monadnock group. Characterized by undisturbed Paleozoic strata and very strong relief — reaching elevations of 3500 feet. The eastern margin is an escarpment facing the Esopus and Rondout valleys which are adjusted to the gently dipping strata of that side. Over the rest of the district the beds lie so 74 NEW YORK STATE MUSEUM flat that drainage is essentially dendritic modified slightly by joint- ing. The great relief of the Catskills is due wholly to erosion of flat but very resistant strata that withstood the destructive ero- sion of Cretaceous peneplanation and stand as residuary rem- nants even to the present time. The Catskills are therefore essen- tially a Monadnock group. In structure they are almost as simple as the higher portions of the cuesta of Long Island, and they hold the same relation to the forms developed by erosion out of the old Paleozoic coastal plain of the interior. Summary Physiographically the most complex zone is midway in the region under discussion —1i. e. The Highlands. This belt is bordered on both sides by less complicated zones of less relief, of more regular topographic forms and less obscure history—— the Piedmont zone on the south and the Paleozoic folds on the north. The outer mar- gins are both simple, essentially eroded coastal plains with strata dipping away from the central belts and on which forms and drain- age lines characteristic of such history are developed. These outer zones are the coastal plain of Long Island on the south and the Catskill Monadnock group on the north. It matters little that they differ in age by almost half of the known geologic column. IOAIOSOI ueyoysy JO jivd & WIIOF OF ST YOIYM Use [][FIOAvOg oY} SSOJOv BuTyOO] suIeJUNOW []PIS}VD IY} JO MIA V CI 93eIg Il GCEOLOGIC PROBLEMS OF THE AQUEDUCT INTRODUCTION The group of studies assembled in this part are chiefly those that have required considerable exploratory investigation in connec- tion with the proposed Catskill aqueduct and that have furnished new data of a geologic character. In some cases the additional investigations have discovered new and wholly unknown structures or conditions and in all cases the features as now established are much more accurately known than would otherwise have been possible. The benefits of the studies have been twofold and reciprocal. On the one side the practical planning of the enterprise has con- stantly required an interpretation of geologic conditions as a guide to locations and methods and on the other the extensive investi- gations carried on have given an opportunity for practical appli- cation of geologic principles under conditions seldom offered and the data secured in additional explorations serve to make the detail of some of these complex features now among the most fully known of their kind. Examples of such cases are (a) the series of buried preglacial gorges (as in the Esopus, and Rondout and Wallkill and Moodna valleys) and (0b) the completed geologic cross sections (such as the Rondout valley, the Peekskill valley, Bryn Mawr, etc.) and (c) the numerous additions to the knowledge of local rock conditions (such as that at Foundry brook, Rondout creek, Coxing kill, Pagenstechers gorge, Sprout brook, and others). Almost every locality has its own specific problem and its own peculiar differences of treatment and interpretation of features. Nearly all of the studies here presented came to the attention of the writer and others! in the form of definite problems or questions involving an interpretation of geologic factors and an application to some engineering requirement. Some of these questions, as is pointed out more fully in part 1, chapter 2, are (a) the location of 1 Professor James F. Kemp of Columbia University and W. O. Crosby of the Massachusetts Institute of Technology and the writer constituted the regular staff of consulting geologists. [75] 70 NEW YORK STATE MUSEUM buried channels beneath the drift, (b) the character and depth of the drift, (c) the kind of bed rock, (d) the condition of bed rock for construction and permanence of tunnel, (¢) the underground water circulation, (f) the occurrence of folds and faults, (g) the position of weak zones, (/) the depth required for substantial con- ditions, and many other similar problems. These need not be treated in their original form. Indeed many of them have now ceased to be problems in any real sense, for sub- sequent provings have made them simple facts, and wholly new questions came to take their places. In some of the larger prob- lems, however, it 1s believed that a treatment which involves a dis- cussion of the original problem and the method of solving it, to- gether with the data thus secured and the final interpretation of geologic features as now understood or established will be more instructive than a mere enumeration of the collected results. So far as possible each problem is treated as a unit and fully enough to be understood by itself. But a general knowledge of Iccal geology as outlined in part I is assumed. CHARTER I GENERAL POSITION OF AQUEDUCT LINE Surface topography constitutes the chief factor in determining the general course of the aqueduct. It is planned to control the water so that it will flow to New York city. There is therefore a gradual descent of aqueduct grade from 510 feet A. T. at Ashokan dam to 295 feet at Hill View reservoir. Wherever the surface of the country is approximately the same as the aqueduct grade for that district it permits of the so called “cut and cover” type of construction which is much cheaper than any other. Therefore, other things being equal, the position that will permit the greatest proportion of cut and cover work would have a decided advantage. Se it is possible from any series of good topographic maps to lay out trial lines that are sure to be worthy of consideration. The topographic sheets of the United States Geological Survey and the niaps of the New York Geological Survey are of great usefulness i such preliminary work. But a little field examination shows that there are many other features and conditions that materially modify even comparative cost and are still more important factors in consideration of per- manence and safety. Sometimes it is not apparent that a course has any objectionable features till considerable exploratory work has been done. Likewise a serious difficulty at one point may more than counterbalance advantages at some other, so that considerable portions of the line are finally shifted to a better average position. In the course of these preliminary explorations much valuable data have been secured that now relate to points a considerable distance off the present line. The information has, however, been necessary and useful. One of the cases of this kind where geologic conditions have had an almost controlling influence is involved in the choice of place of crossing of the Hudson river. It has involved a shift of the whole line between the reservoir and the Highlands. Diff- culties encountered in finding a crossing of the Esopus also con- tributed to the argument favoring a shift of the line [see map of trial lines west of the Hudson]. One of the points where explora- tory work had reached definite results before the more southerly line was finally adopted is near West Hurley. Here wash borings [77] WasH BoRINGS WesT HURLEY LINE atic joes TINY LINE /-Fff, ' | co | Hamilton ses NEW We A \ : \\ Loopus Spales A aN EY EN Yi “ i = = =n - |- Pee ae ne = Zou fb S 5 = . ’ - = «i Onondaga Luneslone Es cs) _——— GEA — Z/ye Bears N.28°wW. YORK ‘ig. 7 Geologic cross section of the Esopus valley at West Hurley as indicated by a series of wash borings STATE MUSEUM were successfully put down through the fine sands and silts of the lower Esopus valley so as to give a fairly acceptable profile of the rock floor [see fig. 7]. Esopus creek in this portion of its course follows the Hamilton shales escarpment which forms a steep border on the west side, while the east border of the valley and floor are formed by the underlying Onondaga lime- stone. Gentle westerly dips prevail for both formations, so that in the perfect adjustment reached before the glacial invasion a cross section would have shown a typical unsym- metrical valley—one side a gentle dip slope and the other a bluff de- veloped by the undercutting of the stream as it shifted against the edges of the shales. Results of exploration show that the valley is filled to a depth of more than 200 feet with silts and sands that are essentially overwash and glacial lake deposits. The flat surface further favors this explana- tion as had been pointed out before any explorations were made. Later observations in that portion of the Rondout valley which is a continu- ation oi this structural feature indi- cate similar deposits as far south as the new line at Kripplebush, Io miles away. In this instance at West Hurley by careful measurement of dips on the Onondaga limestone and the Hamilton shales it was possible to estimate the approximate depth to which the Onondaga floor rock would pass by the time the base of GEOLOGY OF THE NEW YORK CITY AQUEDUCT 79 the escarpment is reached. It was further believed that the cov- ered portion is wholly drift-filled down to the Onondaga. It was easy therefore to estimate the approximate profile and suggest the point of greatest probable depth. The accompanying figure illus- trates the form and structure of this valley. Each valley has had in a smaller way a similar study and adjustment of location of line. The final result is shown on the accompanying map which indi- cates the course of the aqueduct as now being constructed. YORK STATE MUSEUM NEW (Ajddng s9VAA JO pavog, oy} Jo Asojanog Ag) ‘SHOUIOT) PULfOT] YSNOAY) puv ‘OTAALOGqry pur s][Voy Usrpy JO ISOM OY} OF APY V ‘poomry YSnosy) sossed uosoyo AyVuy our, oy ‘Spouuny dinssosd puv ‘ouun} opesd “19A0D puv ynd— uo0T} -nA}SUOD FO SodA} JUdLIZIP S}L YM Pozoopos oUF] [LUY PUe UOTVI0[ 9]qISSOd TOF POADAINS Soul] SurMoOYsS (deur uonwooy 8 ‘S8y wn 0 , 2061 '| AUWANYE OL NOILV9O1 HOd GIAIAUNS SANIT NVMONS (( LONGINOV VIMSLVO ” oe — a memento “Hy Ea ee ORY tt NOLONINOO "ALAN 0? % a? ROUOIOIOIICIOK ICRI EHH # » J? ‘ F r “USOT T tel 1M, nie Vv —— om UASAM ic ‘ i ea trea, N Sh es Sen ce —) Wee) QO sisdaaHnpnod —.: PL a x or CAO TIC), 08 " ty i] Sha Thatta hat Sn * ¢ 5 ¢ “ “i ‘ " ‘ ty 4 \ i ‘ ' PAYA NOUNS ’ iu us* e + 4 ahh ATV MA ‘ ‘ ‘ tN 4 ‘ WNOMOW WHMMH MM uoydig ee me el (@aun) apedg ABAD puke IND CHAPTER II HUDSON RIVER CANYON This is a special study of the Hudson river gorge’ based upon explorations by borings at the several proposed crossings. Alto- gether 226 preliminary borings were made on I4 cross sections. The most important lines of borings are located at seven different points on the Hudson [see location map]. Four of them are in the vicinity of New Hamburg, lying not more than a couple of miles north and south of that village, while three others are located within the Highlands. [See comparative geologic study in following chapter.] The chief basis of information on all but one of these lines is the wash rig, a contrivance as already pointed out that gives rather incomplete data [see Relative Values of Data, pt 1]. On this account it is not possible to give the true bed rock profiles of the river canyon even approximately except at one location, 1. e. the Storm King—Breakneck mountain line. An occasional diamond drill hole has been put down on some of the others and this has _ been done systematically at the Storm King location in a persistent effort to determine the gorge profile and bed rock condition. The work already done has proven that in the Hudson at least the wash rig borings give wholly unsatisfactory profiles. The holes de not penetrate the boulders and heavy glacial drift that is now known to fill the canyon. The profiles, however, that were drawn from this sort of data have some value. They indicate that bed rock is still lower and that the finer silts extend down to these depths. In some places there is a heavier filling of 400 to 500 feet below them before the rock floor is reached. Wherever the diamond drill has succeeded in reaching rock the formational identification has been made and the geological cross section is a little more complete. As a matter of fact, however, at almost every locality the structural relations are so complex or so obscure that they are still not fully known. The accompanying profiles and cross sections summarize the mass of accumulated data: 1 Kemp, Prof. J. F. Buried Channels beneath the Hudson and its Tribu- taries. Am. Jour. Sci. Oct. 1908. 26:301-23. Some of the accompanying de- scriptions of river crossings follow closely this excellent summary of Hud- son river explorations from Professor Kemp. [81] 82 NEW YORK STATE MUSEUM Fig. 9 Key map showing the locations of lines of wash borings forming the basis of the accompanying cross sections of the Hud- son above the Highlands GEOLOGY OF THE NEW YORK CITY AQUEDUCT 83 1 Points of exploration’ a Tuff crossing. This line is a half mile above Peggs point. Wappinger limestone forms the east bank of the river and Hudson river slates the western bank. There seems to be no abnormal structural relation of the formations. All data are from wash borings. The accompanying section gives the results. b Peggs point line. Peggs point is 2 miles north of New Hamburg. At this location Wappinger limestone forms the east bank and Hudson river slates the west bank of the river as in the previous case. The limestone dips gently westerly while the slates have a variable attitude. This is a normal relation and there is no direct evidence of any great structural break. A large number of wash borings have been made and five diamond drill holes were driven, three of them in the river. None indicate a greater depth than 223 feet, although there is a wide stretch, 1040 feet, not ex- plored by the diamond drill. This space must contain the deeper gorge if one exists here. From the known conditions at the entrance to the Highlands, 10 miles further down stream, where the channel is known to be more than 500 feet deeper, it may be rather confidently asserted that a deeper inner channel does exist at this point. c New Hamburg line. This line crosses the Hudson from Cedarcliff to the village of New Hamburg. The river is narrow — only 2300 feet. There are no drill borings within the river channel, but there is one on each bank. Both penetrate Wappinger lime- stone first and then pass into Hudson river slates beneath. How much of a gorge exists here is wholly unknown except in so far as may be judged from the wash boring. There are the same reasons for believing that a gorge exists as those noted for the Peggs point line. Structurally this line is probably the one of greatest complexity. t is however perfectly clear that the abnormal position of the slates and limestone on the east side of the river is caused by a thrust fault. A similar relation of the slates and limestone on the west side must be due to a like movement, but whether they are separated portions of the same structural unit or of two adjacent ones is not clear, although they are probably distinct 1 All of these explorations on the Hudson river have been under the direct supervision of Mr William E. Swift, division engineer, in charge of the Hudson River division. 84 Fig 10 NEW YORK STATE MUSEUM g “y ¥ $ fe) Section LT" Section AVL’. Section MN! a S Wappinger Creek EN « 2 : + ak . OG Sa RK Sv Scoala me Be based upon wash borings. [For locations see key map, fig. 9] Cross sections of the Hudson river north of New Hamburg and of Wappinger creek GEOLOGY OF THE NEW ,YORK CITY AQUEDUCT 85 _ Five lines of wash borings were followed, and the results of these are indicated in the accompanying figures. A maximum depth of 263.5 feet is shown by these wash borings. d Danskammer line. This line is about a mile south of New Hamburg. Two lines of wash borings were made, reaching a maximum depth of 268.5 feet. In this case slates standing almost vertical form the east bank and limestone dipping gently eastward the west bank of the river. Whether there is a deeper gorge or a more complex structure here is wholly unknown. Of the three remaining lines, all of which are within the High- lands, that one projected between Storm King mountain on the west and Breakneck ridge on the east has been much the most thoroughly explored. It is known as the Storm King line. The other two have seemed to merit less attention. One crosses the river from Crows Nest mountain to Little Stony point and Bull mountain just north of Cold Spring, and is known as the Little Stony point line. The other crosses at Arden point about a mile south of West Point and Garrison. _e Arden point line. Only wash borings were made. A maximum depth indicated by this method is 220 feet. Structurally this location appeared to have disadvantages, and although the evidence as to bed rock conditions is confined to the natural out- crops, there is no doubt but that it has objectionable features of this sort. The Hudson follows closely the structural control in this portion of its course. These structural elements include the foliation, the bedding of the original sediments, the subsequent shearing zones, and the strike of folds and faults. Crushed and sheared zones are nowhere in the Highlands seen so extensively developed as on the islands and the east bank of the Hudson in this, the central portion of its Highlands course. The river is very narrow, being only 2120 feet on this line. f Little Stony point line. The river here is 2360 feet wide. The rocks on each side are similar and give no clue to possible depths of channel. Less than 200 feet was reached by the lines of wash borings. Three drill borings penetrated the stony or bouldery river filling somewhat deeper — one near the center reaching 322 feet. None, however, reached bed rock. g Storm King crossing. Extensive exploratory work has been carried on at this point, both on the banks and in the river. Wash borings as usual have given poor results. Two diamond drill holes were run at an angle toward and beneath the margins of the 86 NEW YORK STATE MUSEUM LIME -AILN SovTH RANGE Section ZT 3 Water Sand / Soft Clay = LIME AItN NoRTH FANEE Seclion PIN. Peces Point 2evTrH RANGE Section 0.R Mean High Water an 8 = Fig. 11 Cross sections of the Hudson river near New Hamburg based on wash borings L[For locations see key map, fig 9] GEOLOGY OF THE NEW YORK CITY AQUEDUCT 87 river, and in addition a working shaft suitable for permanent use has been started on each side of the river. These have thoroughly explored the rock character to-a depth of about 800 feet. It has proven to be of constant type, a gneissoid granite, affected by moderate amount of jointing, shear movements and occasional dike intrusion. The two sides are alike, the rock in depth is com- paratively free from water, nearly all coming from the adjacent surface drainage. Persistent efforts have been made to use the drill in the river to explore the rock channel, but with meager results. The difficulties to be overcome in drilling in this tidal river to the necessary depth are probably greater than have even been encountered in any similar undertaking. The disturbance presented by the current, the tide, the depth of water, the drift filling above the rock channel, and the traffic in the river are a constant menace. The complex character of drift filling in this gorge, especially the occasional heavy bouldery structure, makes it necessary to reduce the size and recase the holes repeatedly. But in this regard the work has suffered less actual loss than by the menace of river traffic. Several times after the greatest efforts had been put forth in pushing the drills deep into the gorge a helpless or unmanageable or carelessly guided steamer or scow has wrecked the work. In this way some of the most critical locations have been lost together with many months of labor. The results are shown on the accompanying drawings. It is worth noting that of those holes located far out in the river channel only two have reached bed rock. Even these two have penetrated the rock so little distance that there might be still some doubt of permanent bed rock. The fact, however, that the rock found is of the right type, 1. e. like the walls of the gorge, leads to the conclusion that the bottom was actually penetrated. Neither of these holes are in the middle of the river, and, although the maximum depth of 608 feet was reached by one of them, the central portion of the buried channel proves to be still deeper. One hole located near the middle was able to penetrate to a depth of 626 feet without striking bed rock. But it was finally lost.. The latest results are from a boring that has reached a total deptht (January I, 1910) of 703 feet, the last 8 feet of which was believed by the drillers may be in bed rock. All above is drift and silt. 1 Subsequent exploration has proven that the bottom of the old channel lies still deeper. This boring has been pushed to a depth of 751 feet with- out yet touching bed rock (Oct. 8, I9I0). NEW YORK STATE MUSEUM Van Sk aterm ¢ Ligne Gravel Dock RANGE Secttan Gl. Mean High Frater Cross sections of the Hudson river at four points between Danskammer Light and Fig. 12 New Hamburg [see key map, fig. 9, for locations] (4Jddng 193e\\ jo pavog JO JUoyXo OY} PuL siyeys oy} JO suortsod oy ‘sSurioq paulput OM} js ett FO Poy OY} SUIMOYS SUISSOID SUIS WI0IS 9y} 3e 98108 uospnyy “NIM PeHOUS IVAN ue pane eV ymca Oa Pen AE rN 8 iv ; VI 9}e[q Sen ee ee 94} JO SSUIMVIP WoO, poydepy) ‘SUOT}VIOTdxo HY 94+ JO UOMIOIIP OY} “sSUIIOg [edI}J0A oY} Sur °Y} FO UVOHIS ssoto oVUUeIseIp oytsodu0s vy Ol! MOUNNVANE sr Vern yy eve UAH VP a al VY PRP SOS 1 vy HRN NSO EY aHo YW GEOLOGY OF THE NEW YORK CITY AQUEDUCT 89 2 Discussion The present facts therefore indicate that the buried Hudson channel is more than 700 feet deep between Storm King and Breakneck ridge. Furthermore this is more than twice as great depth as has been found (so far as yet tested) at any other point either above or below this place. Although data of this kind are scarce yet there are two other borings that have given surprising results —(a@) at Peggs point and (b>) the Pennsylvania borings at New York city. Peggs point. At this place, where studies were made for a possible crossing, a hole 700 feet from shore struck rock at 223 feet and the unknown space or interval within which it is possible for a channel to lie is less than 1040 feet wide. This is about Io miles above the Storm King crossing and in much softer rock (Hudson River slates). Yet the Storm King gorge in granite is deeper than that (deeper than 223 feet) for a width of nearly 2500 feet. Of course, there may be, and probably there is, a much deeper channel at Peggs point within the 1040 feet unexplored space. But even so there is a remarkable discrepancy in width of gorge at these two points that must be accounted for in some other way than simple stream erosion. The Pennsylvania borings opposite 33d st., New York city. The data gathered by the Engineers of the Pennsylvania Tunnel Company in their explorations for tunnel from 33d street, Man- hattan, to Jersey City, have recently been made public. There are six holes into rock. Their positions and depth to rock bottom are given below: a 800’ from New York bulkhead 190’ to bed rock = aplite b 1000’ from New York bulkhead 290’ to bed rock = hornblende schist c 2180’ from New York bulkhead 300’ to bed rock = chloritic and serpentinous rock. d 2350’ from New York bulkhead 260'(?) to probable boulder = jasper breccia € 3300’ from New York bulkhead 270’ to bed rock = arkose sandstone f 13700’ from New York bulkhead 225’ to rock—brown sand- stone There are other shallower borings on both sides of the river. Those on the Manhattan side are represented by several different facies of Manhattan mica schist and granite and pegmatite in- go NEW YORK STATE MUSEUM trusives, while the New Jersey side is represented by different varieties of arkose and gray and brown sandstone belonging to the Newark series. It should be noted that although only one hole marks rock bottom as low as 300’ (that one situated 2180’ from the New York bulk- head about the middle of the river), yet there is at least a 1100 foot space on each side which is essentially unexplored, and within one of these spaces there may be a deeper gorge. The cores taken from the east side of this middle zone belong to facies of the Manhattan schist formation, while those on the west side belong to the Newark series. The middle one, however, is essentially a soapstone or serpentine and may be a continuation of the Hoboken serpentine belt. In any case, it belongs in age to the older series of formations. It is certain that here again, 50 miles below Storm King locality, a very deep gorge, if one exists, must be comparatively narrow. Submarine channel. It is worth noting in this same connec- tion that a submerged gorge has been mapped by the Coast and Geodetic Survey on the continental shelf from the vicinity of Sandy Hook to the deep sea margin, a distance of more than a hundred miles. This is interpreted by Spencer? and others with apparently sound argument as the lower portion of the old pre- glacial Hudson gorge formed during an epoch of great continental elevation. The outer portion of this submerged gorge is very deep. That section near shore is shallow and obscure. It has been assumed that this obscurity and shallowness is due to offshore and iver deposition, filling the channel with silt. No better explanation is yet forthcoming. But even here the width of the submerged gorge is suggestive. In very much softer sediments than any en- countered in its whole course on present land, and in a part of its course from 50 to 100 miles below the other sections, the river has cut a gorge only 4000 feet wide at top and 2000 feet deep within a broader valley 5 miles wide. In its deepest known part the proportions are 10,000 feet in width at top to 3800 feet in depth. From this it would appear that the inner gorge type of develop- ment is characteristic of the Hudson, and that it was originally an exceedingly narrow one compared to the present river width, indi- cating rapid erosion during a brief and comparatively recent epoch. This submerged continental margin condition is favorable to the 1 Spencer, J. W. The Submerged Great Canyon of the Hudson River. Aim. Jour Seeh1e05, Vv. 10. (4Jddng 193e\\ jo pieog Aq ydeisojoyq) ‘Aemoyer oy} ye oY} JO punois Sulloyjyes oy} SMoys siy yz “UIe} se Aeqd YsInqmonN se uMOUY FOATI UOSPNFT 9Y} JO JUSWAsivjuS oY], 95108 WOSpnyy oY} pousdsap1sao pue posiejus jeY} 991 [eloe[s Jo onSu0} “UNOU SUP W10}¢ jo odoys AJIOYIIOU BY} WOI, Uses SI 911d GEOLOGY OF THE NEW YORK CITY AQUEDUCT OI assumption that there are narrower, still deeper channels within the unexplored spaces ‘both at New York city and at Peggs point. The only known exception and the one really surprising section is the Storm King crossing. It is too wide, considering the profiles at Peggs point and at New York city for simple normal stream erosion. Thatis clear enough. But a still more difficult question is whether it is also too deep. It is much deeper than any known section above or below for a distance of 50 miles. There appears to be only one satisfactory explanation of this abnormal width of the deeper section and that is by glacial erosion. Just above Storm King is the wide bay opposite Cornwall and Newburgh. The few glacial scratches observed trend about s. 15° e. The ice therefore moved to the east of south, and it is noted that the course of the river is about the same. The northern tront of Storm King mountain is steep and trends east and west while the northern front of Breakneck mountain trends southwest. It would appear therefore that these slightly converging mountain fronts served as sort of a funnel into which the ice was forced from the wide gather- ing ground immediately above, and through which there may have been a tongue or stream of ice of more than average power and efficiency moving almost in direct line of the present course of the river. It is reasonable to expect that these conditions would favor more than average glacial erosion. 3 Storm King—Breakneck mountain profile It is practically impossible to draw a complete profile for the Hudson river gorge at any point in its lower course. Even at Storm King mountain or New York city or at Peggs point, at each of which places considerable exploratory work has been done, only the broadest features are known. Nevertheless, several things have been proven and they are worth considering in this question. They may be summarized as follows: a If there is a very deep gorge at Peggs point (deeper than 250 feet) it can not be over 1000 feet wide. b lf there is a very deep gorge at New York city (deeper than 300 feet) it can not be over 1200 feet wide. c At Storm King, located between the other two and in harder rock than either of them, a gorge at least 400 feet deep is proven to have a width of more than 1500 feet. It is certain that simple stream erosion could not account for such a difference of cross section. There is no doubt but that en- NEW YORK STATE MUSEUM Q2 Poof OOF MO]Oq UOTPeS Sury wa0}¢ °Y} JO oZIS a[qeyxIVus1 34} MOYS ©} a]eos oes 94} 0} UMeIp — A} YIOX MON Yoams pze ye pue sury w40jg ye 4utod S8so9q Je —o3108 uOspnyy ey} FO suorndeas oATFeIedWoy fr “BLT “oor. oan | oa aed cook eae Efe ee tea rt ee | a (| ie Ue — —> pe ces eal eae ie eal SS SS ———————— eases SS SS OS SS Ee Ee = ———} e ~ —————— "o> a "N leq awse Laie SOT > “9 TINNAL VINVATASNNZY FWIONS LIFHLG SEFO MY LAV hi NUMMVHaaM IAM 40 WIGG1W ie wees ec6- a eo ob= 4yooe j AON MNT [ ; = t ye coe ee INS > ado 5 \ \ooe- aT x — Sone AateO |? Gattis] aaa oF aig ssn SS SS SS Ss Op [J x z ° iy 2 4 rn c ees FIIOYy 8 INU WYOLS : 6 ud i) Lite < Al > f a A e x r x a Zz a ry x 4 A F7IONS 4NlOy SIITS GEOLOGY OF THE NEW YORK CITY AQUEDUCT 93 larging by ice so far as widening is concerned is practically proven. It may also be overdeepened, by which is meant that it may have been gouged out deeper than could have been done by a stream of water alone. If ice action then be granted, the profile ought to be and prob- ably is essentially an ice valley profile, 1. e. of a more or less U- shape, rather than of typical stream erosion form. It is certain also in this case, if glacial overdeepening is admitted, that there can be no stream notch in the bottom of it. The significance of this lies in the probability that the floor is approximately the same level on a considerable portion of the bottom, so that when once the margin of this floor is touched the gorge as a whole is thereby- determined for depth. After plotting the borings data and relying upon the factors that seem to be most firmly established, it appears that the following statements are as definite as the facts will warrant: a The average slope of the Storm King side of the valley above river level is nearly 38°, and this is in several steps or sections of steeper and flatter slopes. The Breakneck side is about the same. b The average slope of the Breakneck side of the gorge below present water level (the side on which alone there are enough data > to plot a fairly good curve) does not vary much from this same value [see accompanying profile]. And it is also in steeper and gentler slopes, apparently a series of U-shaped forms set one inside the other, each inner one deeper than the next outer one. Each suc- cessive inner step is approximately 300 feet deeper than the last and 1000 feet narrower. It is certain that this sort of profile is not as simple as at first appears. The surprising feature is the close approximation of the slopes above and below present river level. In view of the fact that glacial widening has been practically proven, as shown before, not much importance can be attached to this uniformity or simi- larity of slope. Ordinarily such a persistence of slope would be taken to indicate simple stream origin, but having abandoned that hypothesis, the value of the angle as a factor in estimating prob- able total depth is lost. In short, one can not assume that the deepest point is indicated by the intersection of the slopes of the two sides. But there is one feature that is at least suggestive. That is the uniformity of the succession of steps and slopes. It was noted above that each successive inner one is about 300 feet deeper and 1000 feet narrower, If this uniformity and proportion is main- YORK STATE MUSEUM NEW 04 “WUIOF JSOWIIUUT 94} JO YJdap o[qeqoid ay} Jo UOT}sossns & PAIS PUL OPIS UTeJUNOU YIuyveIg oy} UO ssurs0oq 9y} Aq pezeoIpul aq 0} Poadotjoq st ‘I9YyJO dy} UTYIIM 9UO ‘suLIO; podeys--) 0} AJUspus} 94 ‘ssutsoq j[edourid ay} fo syydop pue uonedsoy Surmoys syord 931038 uospnyy, ey} yo APHIS V7) 7 VI etal ~1Pd Buiuog 19 Pp2svg ONISSOUD ON! WUOLG ans 40 BMAOY WIBL "o°O6— qyyoee *,Coe- NBAIN vas o 0 0 9 ' il. x ws S x \ Ina 2 ML Wd pees : / vA Va Set S¢/ Lj / J G) VA 0 ) Q r) \ annoys J aLawis \ s°.91 ZZ Oly tS Se ee BIMNY so BIGGIN ct, LawHus Zz3°°3 GEOLOGY OF THE NEW YORK CITY AQUEDUCT 95 tained for the next inner one — inside of holes no. Io and no. 22 —there would be room for only one more and its approximate depth would lie somewhere between 800 feet and goo feet below tide. Recent drilling has shown a marked difference between holes no. 10 and no. 22. WHole no. 10 located 500 feet southeast of no. 22 is nearly 100 feet deeper. Since no. Io is nearly straight down stream this discrepancy is disturbing. But if one considers the distance of each from the east bank it is noted that no. 10 is 900 feet out and no. 22 is 800 feet. Hole no. Io is thus about I00 feet nearer the middle of the stream and allowing for this addi- tional distance according to the profile as known it ought to be at least 70 feet deeper than no. 22. This corrected difference then of 30 feet does not seem to be of much importance. Summary. Everywhere in its lower course the Hudson ex- hibits the character of a narrow gorge, sometimes of a gorge within a gorge, most of which is either submerged or buried several hun- dred feet. | Depths of 200 to 300 feet are average and for the last 60 miles of its course represent widths of 1000 to 3000 feet. Greater depths are believed to be maintained continuously within a narrower inner notch, but of this there is no conclusive proof and very little evidence outside of a few Storm King borings. The Storm King-Breakneck notch is over 751 feet deep. But it is abnormal at least in width and probably also in depth, due to ice erosion. The conditions indicate (a) rapid stream erosion while the con- tinent stood much higher than now, (0) glaciation which enlarged the gorge in at least a few places and filled it with rock debris and later with mud during submergence, (c) finally an emergence with minor oscillations and erosion to the present time. ae 4 Origin of the present course of the Hudson The course of the Hudson is in most respects no more abnormal than that of the Susquehanna. Both flow across mountain ridges in such manner as to indicate their superimposed character. Both date back to the Cretaceous peneplain. But the striking feature of the Hudson is its straight course. As Hobbs and others have pointed out, the river is abnormally straight for more than 200 miles — and this in spite of the fact that it crosses the bedding and other structures of the country rock at nearly all points at an 96 NEW YORK STATE MUSEUM oblique angle. Such conditions are especially notable south of the Highlands where the Hudson cuts at a low angle across the ends of a succession of complex folds of the crystalline metamorphics for 30 miles to New York city. But this is true Only of the east side of the river. The west bank is an almost unbroken uniform escarpment of the Palisade diabase intruded sheet underlain by Newark sandstones, which if laid down upon a pretty well planed Pretriassic surface might easily control the Hudson, and which would not differ from its present course. The most evident exception to this is the course of the river from Hoboken to Staten Island. Instead of following the line of contact between the crystallines and Triassic formations, the river cuts through the crystallines leaving large masses of serpentine and associated schist on the west side. This together with the behavior of the river in cutting across the strike farther north near the Highlands is believed to strongly favor the fault theory of location especially south of the Highlands. The same condi- tions would be favorable to the development of a narrow gorge and perhaps a very deep one rapidly eroded along the crush zone of the fault. From the northern entrance to the Highlands to Haverstraw bay, where the Palisades are reached, the stream course is not by any means straight, but shifts from longitudinal structure to cross structure alternately in a zigzag manner. North of the Highlands the course is more direct again. On the whole the present explora- tions have added little to the facts bearing upon this question. Faults crossing the river are common and easily recognized. Oc- casionally one appears to pass into the river gorge at a very small angle and not reappear. In a few places, especially in the High- lands, the course does not seem to be consistent with the hypothe- sis of a large fault line. It is to be expected that further work at the Hudson river crossing will add materially to the facts relating to the structures within the gorge. CHAPTER JI GEOLOGICAL CONDITIONS AFFECTING THE HUDSON RIVER CROSSING General statement This is essentially a study of the geologic features and cond1- tions shown by exploration to have an important influence upon the choice of river crossing for the aqueduct. In the beginning it was possible to consider that any point between Poughkeepsie and New York might furnish a crossing. The early preliminary in- vestigations showed that it would be desirable to cross either above or within the Highlands and subsequent exploratory work throws light on different possible locations in these regions. Fourteen dif- erent lines were tested by wash borings. Later some of these were tested by diamond drill. As data accumulated it was possible to eliminate many of the trial lines and the more detailed and critical studies became confined to a few important possible crossings. In making a comparison of them as to geological environment it is evident that they fall into two distinct groups’ [see fig. 15]. One, that may be designated the *‘ New Hamburg” group is rep- resented by the “ Peggs point,” “New Hamburg,’ and “ Dan- skammer’”’ lines and is characterized by a series of much folded, faulted and crushed sedimentary rocks, chiefly slates, limestones and quartzites. The other, that may be called the Highlands group, is represented by the “Storm King,” “ Little Stony point,” and the “Arden point” lines and is characterized by crystalline metamor- phic and igneous rock of a much older series. A judgment as to the most desirable crossing involves the selec- tion of one of these groups chiefly upon general geologic features, and finally a selection of a particular line upon minor differences of materials or structure. In the first place it seems necessary to consider, for each group, 1 There have been other suggestions for crossing the Hudson river, farther upstream and farther down than these—one being at New York city — but none have had sufficient claim to attention to encourage much detailed work or so careful consideration as thosé here discussed. A shift of position of the Hudson river crossing involved a correspond- ing shift of a large section of the northern aqueduct line. The first choice of location occasioned a shift southward of all that portion between Ashokan reservoir and the Hudson. [97] STATE MUSEUM NEW YORK 98 ISAT UCSPN}FY sy} JO SSuisso1d ojqissod se paIpnjs soul] aArT}eusd}]e Surmoys dew ouyjyng Sr “Brg SAIN 2 Uae aa t > | wes oe 2061 ‘| ANVANYF OL > aa = NOILV9O1 YO4 G3ASAHNS S3NI1 \ \ \ LONGANOV TIIMSLVO \ LOX \ ) = \ \ soni ae FOVTITIA TITUS OX, 3 oN Ye \ eee > cag Ny @ cee im STTVA AYAONTAA VM” ett” eg Saad Pe a wee \ SA é WS % SUDA NVH Md AN J Og = TTIMHS14 ZEN _—- - — * was ——— Qe es = OUNAMAN Oy i XXX KKK eee ee LOUIS of = em ee: jauuny apesg ane 438A0D pue yng (a ae el aa —o~ unio /) ae = ; 7 SMS SHINNOD GNV19UI onuanne: GEOLOGY OF THE NEW YORK CITY AQUEDUCT 99 the whole length of pressure tunnels whose position would be modi- fied by a shifting of river crossing. This is because the aqueduct will approach the Hudson with nearly 400 feet head —i. e. 400 feet above river level or with an equivalent pressure. For this reason it is considered necessary to plan a rock pressure tunnel beneath the river which can deliver the water at nearly the same elevation again on the east side. | Thus any one of the “ New Hamburg group ”’ involves a contin- uous pressure tunnnel reaching from the margin of Marlboro moun- tain to Fishkill range, a distance of approximately seven miles, while any of the ‘“ Highlands group” permits the substitution of two more or less separate siphon tunnels (Moodna creek and Hud- son river) of considerably less combined total length. A reliable conclusion as to the choice of crossing is probably best reached through a comprehensive understanding of the geologic de- velopment of the region together with a consideration of specific local conditions. With this end in view a condensed outline of geologic history, so far as it bears upon the questions at issue, 1s inserted. But for a more comprehensive discussion of these matters the reader is referred to the explanatory chapter of part 1. ’ Geology ; This particular locality, including as it does the Highlands of the Hudson and the district lying along its northern border, is one of the most complicated stratigraphically and structurally to be found in the entire region. The strata represented include more than half the total geologic scale reaching from the oldest sedi- ments following the Archean up to and including a part of the Devonic series [see pt 1]. The rock types include granites, diorites, gneisses, schists, marbles, serpentines, slates, quartzites, sandstones, limestones, shales, and, less extensively, other varieties. And the region bears the evidence of no less than three periods of mountain- making disturbances, each in its turn adding to the succession of. foldings, faultings and unconformities. The oldest formation is a crystalline gneiss —a characteristic rock of the Highlands. It represents an ancient sediment that has been completely recrystallized during some of the earlier mountain- making period. It is older than the Cambric. Interbedded with it to a limited extent are quartzite beds, ancient limestones (now usually serpentinous in character) and schistose beds; and in it are many igneous injections, mostly granites of various types. All 4 100 NEW YORK STATE MUSEUM these igneous injections are therefore younger than the gneiss and are very large and abundant in certain cases. The granite of Storm King, Crows Nest and Breakneck ridge belongs to this type. Following the sedimentary cycle represented by the above series, and perhaps others not now preserved, the region was folded into a mountain range, the series was extensively metamorphosed and passed through a long period of erosion during which it was again reduced to sea level position and began to accumulate a new series of sediments. The lowest beds occurring upon this foundation are sandstones, now changed into quartzite. In places they are conglomeritic, and may now be seen projecting into the valleys along the Highland border. This formation is of Cambric age, and is from 200 to 600 feet thick in favored places. It forms an almost continuous belt along the north side of the Highlands except where cut out by faulting, and extends with similar breaks beneath the later sedi- ments northward. This quartzite is known as the “ Poughquag.” Upon the quartzite of this series there was developed a succes- sion of limestone beds at least 900 to 1000 feet in thickness. This formation is known as the “ Wappinger”’ and includes some beds that are of Cambric but for the most part of Ordovicic age. The final member of this series is a shale and shaly sandstone in places changed to slate. It is quite variable in actual character and has a great thickness, never yet successfully estimated, but probably several thousand feet. This is the so called “ Hudson River slate” series. In this region they are of Ordovicic age. This is the succession which the proposed Hudson river lines has to penetrate in a pressure tunnel. Later Siluric and Devonic strata lie in the immediate vicinity of this alternative line, but add no complication to the problem as it now stands. Therefore no other formations need be considered except the glacial drift. This covers almost every rock surface and is deeply accumulated in some places, notably in the narrow gorges and valleys, obscuring the finer original topographic lines. A summary of the history of the formations chiefly involved in this problem with a suggestion of later erosion activities may be tabulated as follows: Glaciation Reelevation Erosion (interrupted) Elevation (rejuvenation) Cenozoic GEOLOGY OF THE NEW YORK CITY AQUEDUCT IOI Erosion to peneplain OP CA ie ponte ar ae Unconformity A long interval including two mountain-making epochs and at least one period of general sedimentation Mesozoic {Hudson River slates Ordovicic } aloo ee limestone | Poughquag quartzite reeterd he ae Unconformity A long interval including mountain folding, igneous injection, erosion, and perhaps other sedimentations : Cambric Paleozoic The metamorphosed schists, limestones, quartzites tc., together with accompanying intruded igneous masses — forming the basal gneisses of the High- lands 3 Proterozoic The evidence of such succession and history gathered from the scattered outcrops of rock in the immediate area, is nowhere better shown than in the field covered by this investigation. Structure When such outcrops as are known are plotted and organized, sev- eral important facts become clear. 1 The folds run with remarkable persistence northeast and south- west. 2 The succession in many places is not normal. Often a whole formation or even two of them are missing and formations that should be separated are brought side by side. Faulting therefore is prevalent and the occurrences show that these ee fault lines usually run northeast and southwest. 3 A consideration of the dips of the strata shows that most of the folds are overturned as if pushed by some general movement from the southeast. 4 This same movement causes the faulting to be largely of the overthrust type, and in some cases the lateral displacement attained in this way may possibly be several thousand feet. 5 Isolated “islands” of the older rock formation appear out in the later sedimentary area. They all seem to belong to prolonga- tion of the ranges of the Highlands and their abundance undoubt- 102 NEW YORK STATE MUSEUM edly complicates the underground structure throughout a consider- able belt. ; ; 6 The Highlands area terminates in a serrate margin which, in the latest thrust movements from the southeast, must have created very unequal distribution of stresses within the slate-limestone region to the north causing additional cross folding and faulting. For the most part these can be traced only a short distance before losing their identity. In a mountain folding movement, the uppermost rocks are most broken and displaced or crushed while those of greater depth may be bent or uniformly folded or even recrystallized. It would ap- pear that this latter was the condition of the Highlands rock series during its earlier history. And even in the latest movements its lines appear to be less radically disturbed than the slates and lime- stones to the north. Most of the disturbances that invite serious consideration belong to the latest period of these mountain-making upheavals. Comparison of routes 1 New Hamburg group. This group of crossings is in the later sedimentary series. Hudson River slates and Wappinger limestone are the chief formations. But within the southern third of the tunnel, at least, the underlying Cambric quartzite and the older Highland gneiss would be cut —the quartzite possibly three times. The succession therefore will be of considerable complexity as a whole. All of the formations involved are thrown into very steep dips at most places and are consequently liable to rapid and unexpected changes — some of which probably do not show at the surface. There are several fault lines belonging to the major northeast and southwest series to be crossed by such a tunnel — one of them in each case being met at considerable depth and beneath or adja- cent to the river. These faults besides being the weakest zones of rock as a rule, are in addition the most unstable in any possible future earth movements. Although there is no evidence of recent displacement along these lines, still such a thing is always possible and recent serious effects of this kind on the Pacific coast suggest caution. It is manifestly advisable, if possible, from every stand- point to avoid crossing several of them. In the field there are numerous springs of very large flow along many of the limestone borders. The concentration of them to these situations in addition to the occurrence of an occasional sink- GEOLOGY OF THE NEW YORK CITY AQUEDUCT 103 hole, leads to the conclusion that they are more intimately depend- ent upon the limestone structure for their existence than upon the glacial drift or any superficial factor. Their abundant flow, some- times on high ground, indicates rather extensive structural con- nections and this is believed to be the limestone bed itself and that such flows would be encountered also in depth. The occurrence of sinkholes suggest also possible solution channels and cavities and distant outlets. The types of rock to be encountered on the lines represented by this group are easily workable. Among them all the Hudson River slates is probably the most satisfactory from any standpoint. It is generally easy to penetrate and has a capacity for healing its own fractures. For this reason it can be considered good ground, tight and safe. But a considerable distance of the tunnel can not be kept in slate—perhaps even more of it than can be proven from surface observations. The other formations are con- siderably less satisfactory. The limestones are in places shattered and are liable to abundant flow of water. The quartzite is ex- tremely hard, as difficult to penetrate as granite, and where crossed by the faults is probably not healed at all, while the gneiss is doubt- less of similar character to that of the Highlands crossings to be discussed later. Only minor modifications result from a choice of the individual crossing, whether “ Peggs point,’ ““ New Hamburg,” or “ Danskam- mer.” In one of them, New Hamburg, it would appear possible to cross the actual river section wholly in slates. This seems to be the reasonable conclusion from the diamond drill boring at Cedar Cliff. But even that line necessitates crossing at least two fault contact lines immediately at the east bank and beneath Wappinger creek at depths not immensely less than that below the river itself and both wholly within the range of influence of the river waters. It would appear therefore that the situation is not materially altered in the present discussion, no matter which particular crossing of this group is considered. 2 The Highlands group [see cross section]. In this group of crossings there are two separate features to consider. (a) the Moodna creek valley which these lines all cross, and (D) the Hud- son river itself. Their characteristics are as follows: a Moodna creek |see separate Moodna creek discussion]. So far as known Moodna creek can be crossed almost wholly in slate. It is possible that the underlying limestone may come near enough * to the rock floor of the valley to be penetrated but there is little I04 NEW YORK STATE MUSEUM direct evidence of it. The ancient valley is deep and probably marks a line of displacements which can not be avoided, no matter what route is chosen. The fault contact at the border of the High- lands is not expected to prove troublesome as it seems very tight at the exposures seen. The buried granite ridge (a continuation of Snake hill) which underlies the western end is now known to come within the limits of the tunnel and adds one more complication. Except for the fact that the ancient Moodna valley is deep and filed with heavy drift that is unusually difficult to prospect, there would seem to be no source of special trouble. It has no lines of weakness that are not also present in the more northerly districts and the tunnel has chances of crossing them under more advan- tageous conditions without so much complication with the lime- stone series as. characterizes the New Hamburg group. b Hudson river. Among the Highlands group of crossings there is considerable difference of structure dependent upon the exact location of the crossing. The conditions that prevail may be sum- marized as follows: (1) Storm King location. This is wholly in massive and gneissoid granite. The rock is the most massive and substantial body of uniform type found in the Highlands. The course of the river indicates some weakness in that direction. This weakness may be some minor crushed zone or even the jointing alone that prevails throughout the exposed cliffs. But there is no direct evidence of faulting, cutting the line and such crushing as may be encountered is believed to have originated at such depth and under such conditions as to cause no large disturbance. The freedom of this formation from all bedding structures and natural courses of underground water circulation on a large scale is an additional factor. There is absolutely no other place, within the region, where the Hudson river can be crossed from gradé to grade in good ground of a single type with so great probability of avoiding all large lines of displacement. (2) Little Stony point location. The conditions that prevail at this point are similar to those that characterize the Storm King line. The only known difference is in the considerably more shattered condition of the granite, especially on the west shore at Crows Nest. It is estimated that this crossing is less favorable by reason of just this poorer condition of the rock and the somewhat greater yielding to regional disturbances that it seems to indicate. (3) Arden point or West Point location. Qn this line the river would be crossed in the gneiss series proper instead of in granite, (Ajddng to}v\\ Jo psvog Aq ydeisojoyd) ‘apis jsvo oy} UO JUuLOd MOT {][vUIS dy} ‘JUIOg AUOJS o][}IT] OF JSOM oY} UO JSON SMOID WOA} SOSSOID YOIYM OUT] JULIO AUOJS 9H] OY} PUL “opis sv DY} UO UIVJUNOLU possns oy} ‘YOoUYVoIg, O} BSuIYOvod OUI] SUIS{ W40}G 9Y4}— dvs sty} Ul ot] Ssurtsso1s pasodoid oy} Jo OMT, ‘JUIOG JSOM\ WO YJIOU SUIYOOT Udos sv spuLTySITT oY} OF AVMo}LS UILJUNOW YIUVOSE — SULY WA40IS OY, CAS Se tas mM QI 93¥I1d GEOLOGY OF THE NEW YORK CITY AQUEDUCT 105 It is largely an ancient stratified series much metamorphosed con- taining belts of interbedded limestones, quartzites, and schists, in addition to the more substantial feldspathic gneiss. The eastern bank of the river bears also abundant evidence of extensive crush- ing and shearing and is believed to indicate a displacement in this zone. For these reasons the West Point crossing is considered an unfavorable route compared to either of the others of the High- lands group. ) Summary. In a comparison of the geologic features that are of most importance in contrasting the possible routes for the Hud- son river crossing the following points are considered of most importance. 1 The New Hamburg group of crossings involves (a) the long- est tunnel, (b) the more complicated structures, (c) the greatest number of known faults, crush zones, and related disturbances, (d) the more variable series of rock types to be penetrated, (ec) the greater tendency to encounter heavy underground water circula- tion, (f) the greater probable susceptibility to disturbance from future earth movements, and (g) the greater number of uncer- tainties of rock relations. 2 In contrast the Highlands group admits of (a) shorter totai tunnel length, (b) the most profound fault lines of the district are crossed either in high ground or are avoided or, because of the rocks involved, promise the least possible trouble, (c) the Hudson river itself can be crossed in a single formation with probability of avoiding lines of largest structural weakness confining the greatest pressures and deepest tunnel work within the most uniform and substantial rock of the whole region. There are, of course, many unknown or only partially known features obscured beneath the covering of drift or lying beneath the river itself; but, however many there may be, it is not believed that they can materially change the general situation. The major characteristics are so well marked that any addition to those already known would in all probability increase the difficulties of the New Hamburg group of routes at least as much as and perhaps more than those of the Highlands group. In view of the above facts and inferences the judgment has been in favor of the Highlands group of crossings as the more defensible on geologic grounds as a route for the aqueduct line. Furthermore, in accord with the preferences already noted, the Storm King loca- ticn is regarded as the most likely to give satisfactory results. 106 NEW YORK STATE MUSEUM Quality and condition of rock The rock of Storm King mountain and of Breakneck ridge at the Hudson river crossing is a very hard granite with a gneissoid structure of variable prominence. The color varies from grayish to light reddish and the structure is always coarse passing into pegmatite facies that occur as stringers or irregular veinlets. The grayish facies is of slightly finer grain and more gneissoid. Those portions that have been sheared are still darker. There are many joints at the surface running at various angles and an occasional slickensided surface. The mass is cut by several dikes of more basic rock (diorite) of widths varying irom a few inches to 8 feet. These dikes are somewhat more closely jointed than the granite and consequently a little more readily attacked by the weather. But where protected they are equally substantial for underground work. The chief variation from this condition is where crushing or shearing has induced metamorphic changes. Wherever bed rock has been reached at this point and to such depths as workings have penetrated the rock is of this type. The work includes (@) four inclined drill holes from the river margin — two starting from the surface and two from chambers set off from shafts at a starting depth of about 200 feet, (b) several vertical holes in the river itself, and (c) two large working shafts 20 x 20, one on either side of the river. _ These give all the data? known as to the condition at depth. From them it is apparent that crushing and shearing have been prominent. Many splendid specimens of crush breccia are thrown on the shaft dump. But its present condition at the depth involved is sound and durable. The fractures are rehealed. There has been a recombina- tion of constituents giving a new matrix of complex silicates among which epidote is the most characteristic, while simple decay is of little consequence. For strength and permanence the conditions could not well be improved. There is no reason to apprehend any change for the worse for the reason that the same tendencies must prevail at that depth throughout. It would appear therefore that faulting movements, or the existence of a fault zone of importance can not become a serious obstruction, because of the tendency to 1Since this paragraph was written four inclined diamond drill borings have been made from chambers at depths of about 200 feet am the shafts. These have now penetrated the whole distance beneath the Hudson with very satisfactory results. (Ajddng 10}e\\ JO plvog ‘JoOr ‘oz AJOqUIDAON Uoyr, Yydvisojoyd) ‘sulsoq Asojze1O[dxd Ul posvsud Ssit [[IIp Jo our, oy} Aq JouUN) oAnsso.sd posodoid oy} JO UOT}VIO] OY} Surmoys ULrejuUNnOUL YOoUyeowigG Wot} JIATI uOSphy_y 9Yy} Purv UleyUNOW SUIS, UWIOVS SS —" pesse, GEOLOGY OF THE NEW YORK CITY AQUEDUCT 107 heal up the fractures and so make the rock about as substantial as before. It is noted elsewhere that faulting is common in this region, and that in a considerable portion of its lower course the Hudson prob- ably follows such structures. It is, however, wholly unnecessary to assume that its whole course is a fault line. Whether or not there is a longitudinal fault zone of any prominence in the river at Storm King is unknown. There are several cross faults, both above and below this point, that give much clearer surface evidence of their presence. Fault zones have proven to be objectionable ground in many places along the aqueduct line, but elsewhere the. data refer chiefly to situations favoring more ready underground cir- culation, i. e. at higher levels. In this particular case the rock in question lies below former ground water level within the belt of cementation rather than up in the belt of decay, and there is prob- ably no disintegrated rock from any cause. = ¥ i ia ¥ ¢ - ot eo : . v4 i a) + Shy = ere?) 7 CHAPTER IV GEOLOGICAL FEATURES INVOLVED IN SELECTION OF SITE FOR THE ASHOKAN DAM Topographic features of the southeastern margin of the Cats- kills, where the chief water supply is available, fixes the approxi- mate location and bounds of the principal reservoir. The accom- panying map, a portion of the western part of Rosendale quad- rangle, shows the situation. The part of the work involving the chief geological problem was the choice of the principal dam sites on the Esopus. This is known as the Ashokan dam. This part of the Catskill system belongs to the Reservoir Department under Mr Carlton E. Davis as department engineer. There were originally considered three sites: (1) at “ Broadhead bridge,” (2) at “ Olive Bridge,” (3) at.“ Cathedral gorge” or the “Tongore” site. Any one of these seemed possible from a topo- graphic standpoint. Later developments in regard to storage ca- pacity and engineering considerations finally reduced the practicable sites to two—the “Olive Bridge” and the “ Tongore.” These were then explored thoroughly as an aid to determining whether or not there were favorable or unfavorable conditions at either location. Trenches were dug, shafts were sunk, wash holes were put down, and drill borings were made. The amount of such work done was sufficient to show the actual conditions both of the drift and bed rock and incidentally to throw some light on minor matters in geologic history. This discussion is essentially a summary of these data and a com- parison of the geologic conditions indicated by the explorations’ of these two sites and a statement of some of the geologic character- istics of the area. 1 General geologic conditions as shown by the explorations Bed rock is dark colored Devonic sandstone and shale, the Sherburne formation, lying almost horizontal, strongly jointed, plainly bedded, and of good quality for the foundation of the dam. At both locations the present Esopus flows in a postglacial gorge 1Jn this work of exploration a very efficient staff of engineers was engaged. Among those having very much to do with the features here discussed are Thaddeus Merriman, division engineer, J. S. Langthorn, division engineer and Sidney Clapp, assistant engineer. [ 109 ] iio NEW YORK STATE MUSEUM and there is a somewhat deeper buried channel a short distance to zesS fresh and substantial, due to ionmer weathering, than the pres- ent exposed surfaces. In each case glacial deposits reach a thickness of more than 200 feet within the narrow valley or gorge, especially along the north valley wall within the lumits oi the proposed dam. Special geological conditions. The factors in which there is most variation and which are of most significamce in a comparative study are those belongmg to the glacial drift deposits. In order to properly estimate the influence oi some of these features it will be mecessary to briefly consider the types of material represented at different places and the conditions under which they were fonmed. Types of material Till. Heavy bouldery wll, mixed clay, sand, gravel, and boulders, is the most abundant type of materml. It forms especially the chief surface material throughout the region, and is the surface type at both sites. It becomes at places quite sandy, but 1s almost everywhere good, impervious material because of its mixed character. Laminated till. At a few places, notably m the Beaver kill near its mouth, and m a trench above Olive Bridge, and im the “big drgway~ above West Shokan, strong lammation appears in heavy stony till as 1f laid down rapidly in comparatively quict water such as the margin of a lake. This material is especially mmpervious. Gravel hillocks. A few small illocks with moraimic contour, indicating a dumpmg ground for some glacier of a small scale, occupy the flat mmediately wesi of Browns Station. They were, at a very late stage, piled mito the course of a former glacial stream whose delta deposits occupy the sandy bench above the 500 foot contour just north of Olive Bndge. Assorted gravel and samd. This material is abundantly developed just north of Olive Bndge. It seems to have formed a delta de pcesit at the mouth of a glacial stream that emptied mito the mam valley at this point The running water washed almost all of the clay and extremely fme material farther out, where they settled m the bottom of a small glacial lake that was at that tome held m this upper portion of the Esopus valley. The dam that held im this body of water which reached above the 520 foot lime stood near the proposed “Olive Bridge” dam site. The materials fonming the dam were im part the glacial till that is now found on that site and (A[ddng 19}e AA JO prvog Aq ydersojoyg) ‘(ueyoysy) Wep osplig SAITO 7@ SerVys pue SouoyspueEs oUINGIoYS 94} UL YOUII} JoO-jnyD gI 93eId (oe _—=— SS ee x = MARCH 17,/908. 200 ae ES SEs ==> >> SSS = ot Seas Vessel TS SS ee SS © Bornes. Section of Site on Centerline Corrected fo Jon. 1909. Fig 16 Location of the Ashokan dam at Olive Bridge site and a geologic ’ cross section. The small dots in the plan indicate exploratory borings. The section shows the rock profile indicating a preglacial channel of the Esopus. The present Esopus flows in a new postglacial:channel at a higher elevation. The lowest materials in contact with bed rock are heavy stony till, laminated till and stony laminated clays —all good impervious material wherever exposed and tight upon bed rock. Sands and laminated clays are extensively developed immediately northward of the site and streaks of these deposits interlock to a limited extent with the till materials of the site itself, but they do not extend far and die out in wedges among the heavy deposits that characterize the southern slopes of the hill forming the northern terminus of the dam. These pervious streaks do not extend at any point con- tinuously through this hill and consequently as a whole the present barrier as it stands is practically impervious. The poorer materials (assorted gravels and sands) characterize the upstream side, and the better, more impervious materials (till and laminated boulder clays) characterize the downstream side of the proposed Olive II4 NEW YORK STATE MUSEUM Bridge site. It is therefore advisable to locate any such structure as adam ata point as far down stream on this site as other engi- neering factors permit. b “ Tongore” site. At Tongore, bed rock is at least a hun- dred feet deeper than at Olive Bridge. In the deeper parts, below the 400 foot line the deposits as indicated by the wash borings [see sections] are interpreted as a fairly continuous succession of till, stratified sands and gravels, and laminated sands and clays belong- ing to two or three different stages of accumulation. Upon this the heavy upper till was laid down. It is believed that the records fully support this view and that the stratified or laminated materials were accumulated at a time when a temporary dam existed at some point still farther down the Esopus valley. It is apparent further- more that the most porous zone is at the junction of the upper till and the lower stratified deposits and in part is represented by the assorted pebbles of stream wash —1in general not far from the 400 foot line. These middle zone deposits are believed to extend continuously through the drift ridge that forms the northern half of this site. As before noted, though rather impervious vertically, aay M yp Fig. 17 Plan and geologic section at the Tongore site. The dots on the map indicate exploratory borings and the course of the buried channel of the preglacial Esopus creek is shown making a right angle bend to the north. The section shows the buried chan- nel, the new postglacial channel and the great accumulation of porous modified drift- which is regarded as one important objection to this site for the dam. some of these deposits allow ready lateral movement of water. This is held to account for the rather persistent occurrence of springs or seepage along the creek bank at about this level both above and (Ajddng 103¥\\ Jo pivog Aq ydeisojoyd) “}flip JO Joo} One YJVousd poLind Aod[[vA 9Y} JO apis yOu dy} Je Sol oss00 [eovjsoid sy, ‘OHS W1O0SuOT, oy} ye Yootd sndosy jo jJUswYyUsIjUo [eIvisjsod eV ‘9d105 [BIpsyye) O% 93e[d T5 GEOLOGY OF THE NEW YORK CITY AQUEDUCT ‘OHS OSPlIg PANO [VAI oy} J puNoy o19M ULY} SUOT}IPUOD dI80JO9S Jo100d JUasoIdo1 ‘ssauSNOrAIEd I1aYy} JO IsNRd9q ‘YOIYM ‘UOTVVIO] SIY} SUIZIoJOBIeYS Spuvs PoyHe‘]s snonurjUo0D pu IAISUd}XI BUIMOYS dS I10SUOT, dy} Je JOPBILYD JJLIpP JO [Iejaq QI “BHT Woy NE WEI Y BOS IYO gS St 7) de ra Wee. Toi ee PPWNAOAIS Wo i @PPIArriwy 2274" dz vpepr MN arte) ooee7 8 8 . “N i wo WT SIRIVEI rede se ft RPS ries Oh SOR Pps CALE PRI SI NIE CT S geoscz PVG P21} (OAS W195 Aa PING Jo WE, DLA "IP? O9O8/K/ 4-2 HO“UIES 116 NEW YORK STATE MUSEUM below the site. The great thickness of these laminated beds, in places a hundred feet or more, together with the abundance of sand in them, and the caving tendencies exhibited by them in one of the large shafts, indicates poor conditions for such a piece of work. The behavior of one of the test shafts throws some light on con- ditions within the drift deposits. At this place after sinking into the underlying gravel beds there was “no water” at first, but after going a few feet deeper there was an abundant flow, that did not rise much in the shaft. This case seems to support the following interpretation. The gravels encountered do not form an isolated pocket or lens, else it would have carried water full from the first. It must be a fairly continuous porous zone with large feeding connections else it would run dry, and it must have an easy discharge else it would have risen above the level of the first gravels. Therefore it must be a rather well marked subterranean water passage or porous zone of considerable extent. Such conditions would make an impervious core wall to bed rock at this site a necessity and its construction a matter of considerable difficulty. At this site also because of the small cross section of the ridge, there is little chance for the inter- locking of layers or the blocking of the porous ones by a till barrier to check the lateral seepage, and there is no chance to move farther down stream to secure such conditions. 4 Summary Because of the (a) higher bed rock throughout, and (6) the more uniform and impervious quality of drift deposits, and (c) the more massive cross section of drift barrier for foundation, and (d) the perfectly tight contacts of till and bed rock, and (e) the limitation of the more porous materials to higher levels and (f) the glacial history connected with the development of all these parts, “ Olive Bridge” is the preferable location for the proposed Asho- kan dam on Esopus creek. CHAPTER V CHARACTER AND QUALITY OF THE BLUESTONE FOR STRUCTURAL PURPOSES Probably no stone marketed in New York State is more exten- sively known than the “bluestone” of the Catskill region. But it is noted particularly for a special purpose, 1. ec. as flagstone, because of its capacity to part or cleave into thin slabs. These slabs are proven by experience to have remarkable weather resistance and durability. Little attention has been given to the question of dimension stone —whether or not such blocks of as high quality as the flags could be obtained and where such quarries could be opened. There are several reasons for this situation. In the first place (1) the stone is of a dark color and has a dull appearance so that it is not fancied for the usual expensive structures where large sizes are used, also (2) the quarries are small, shallow, and are worked on a small scale by single individuals or groups of neighbors with few quarrying tools and no transportation facilities for large mate- rial, and in addition (3) considering the work and equipment neces- sary and the demand the flag industry was more profitable. Because of the large demands of the Ashokan dam where nearly a million cubic yards of heavy masonry construction are to be used an entirely new situation has developed. It is especially desirable that a rock capable of furnishing heavy dimension blocks should be discovered. The usual slab or flag type is unsuited to a consider- able part of this work. A study of the adjacent region therefore has been made and explorations along certain promising lines have been conducted to sufficient completeness to prove that a suitable stone can be furnished in large quantity. The characteristics of structure and occurrence as shown by this special study are given, together with some of the later exploratory data. Physiographic features?! All of the rock formations are sedimentary, chiefly sandstones and shales. They lie in alternating beds of variable thickness and are almost horizontal. The total thickness is many hundred feet so 1 The principal argument of this discussion has been used in a previous article by the writer under the title ‘‘ Quality of Bluestone in the vicinity of the Ashokan Dam” in the School of Mines Quarterly, v. 29, no. 2. 117 118 NEW YORK STATE MUSEUM that neither the bottom nor the top beds of the series are to be seen in this locality. The region is one of considerable relief representing preglacial erosion. The glacial drift mantle has modified it chiefly by obscur- ing some of the smaller irregularities of rock contour, and espe- cially by partially filling many of the stream gorges. Postglacial erosion has not completely reexcavated the old channels. But the contour of the uplands reflects the character of the bed rock with considerable success. The tendency of the more massive and coarse grained varieties of rock to resist weathering and erosion more suc- cessfully than the finer grained and more argillaceous or shaly facies is a general characteristic. Since these varieties form suc- cessive or alternating beds throughout the whole area, the result is an almost universal cliff-and-slope surface form. This bed rock topography is somewhat obscured but not wholly obliterated by glacial erosion and deposition. Therefore it may be used with con- fidence in locating or tracing the more durable beds since they almost invariably appear as a shelf or terrace with a steep margin toward the lower side and a gentle slope on the rising side. Structural features The rock types include bluish gray or greenish gray sandstones with almost horizontal bedding, and sometimes exhibiting cross- bedding structure, and compact very dark argillaceous shales. These two are of about equal prominence, but only the sandstone is of importance in the present discussion. Its minute structure will be given in greater detail in the petrographic discussion. Jointing is common and persists in two sets nearly at right angles to each other — one striking northeastward and the other toward the northwest. In some of the best exposures, these joints are clear-cut and run Io to 18 feet apart, dipping almost vertically. In the more massive beds there is very little small jointing, so that the character is especially favorable to large dimension work. But still more prominent structures are the partings which follow the bedding planes. These give the rock a decided tendency to cleave naturally into slabs, the uppermost exposed portion of almost every outcrop exhibiting this slab structure in more or less perfec- tion. So general is this structure at all horizons in the sandstones of the series that there can be no doubt of its connection with some original sedimentation character. Besides it is a potential factor in nearly all the beds even when not very apparent. The (Ajddng Joye \A JO preog Aq yders0j0yq) ‘sjulof JO SjoS JuoUTUOId pue Ie[Nse1 AIZA OM} PUL SUIPpaq [ejUOZIIOY IY} SuIMOYS ‘ssey sUINGIoYyS IY, ' GEOLOGY OF THE NEW YORK CiTY AQUEDUCT 119 exposed places exhibit the character so prominently only because of the weathering effect, which develops the natural tendency. This general conclusion is borne out by the well known practice of quar- rymen of the district of splitting the larger blocks into slabs of the required thickness by wedges driven along certain streaks that are known as “reeds.” A reeding quarry is one that has this capacity well developed, and it is this character in part that has made the “bluestone” or “ flagstone”’ of New York an important factor in the production of the United States for a great many years. For large size dimension stone where great stress is involved it is evident that this structure would not be desirable. These definite planes of weakness reduce the general efficiency. A little observa- tion however shows that there are some outcrops and an occasional quarry where the more massive blocks do not split well. From the necessities of the industry these have been avoided or but meagerly developed. In some cases of this kind the sedimentation is of the cross-bedded type with somewhat interlocked laminae. If the grain is coarse such varieties resist splitting with great success. The thickness of such beds varies from a few feet to 25 feet or even more without prominent interbedding of shale layers. | Stratigraphy. These are the sandstones, flags and shales known as the Hamilton, Sherburne and Oneonta formations belong- ing to the Devonic period. The strata of the immediate vicinity of this examination belong to the Sherburne subdivision, but no at- tempt to differentiate the formations was made. Structurally and petrographically the different formations are not distinguishable in this area. On the market the stone from either is known generally as “ Hamilton flag” or “ bluestone.” Economic features There are hundreds of quarries in this general region. Nearly all are small, and are worked on a small scale without machinery. The product is almost wholly thin slabs of the flagstone type. This is supplemented by a small amount of somewhat more massive char- acter, dressed for window sills; and a very limited output is of dimension stone of larger size. The general lack of suitable me- chanical devices and transportation facilities are the chief reasons for the limited output of the last named grades. Petrography The basis of this discussion is a microscopic examination of sev- eral thin sections made of the different types of rock from the I20 NEW YORK STATE MUSEUM quarries whose field geologic features give promise of encouraging results. The most characteristic variations are illustrated in the accompanying photomicrographs, plates 22, 22. Texture. The rock is granular, the individual grains varying from minute particles in the finer shale layers to three or four tenths of a millimeter in diameter in the coarser sandstone [pl. 23, lower figure]. The grains are seldom rounded. Jagged or frayed or elongate forms are the rule [pl. 23, upper figure]. There is no marked porosity. When the rock was first deposited as a sediment it probably had the usual large interstitial spaces of such rock type, but in this case some subsequent modification — an incipient meta- morphism — has largely obliterated the voids by the introduction or development of mineral matter of secondary origin. In general it is quite apparent that the average grain was orig- inally more rounded than its present representative. Mineralogy. The original minerals in order of abundance were the feldspars, quartz, and probably hornblende, biotite, and in much smaller amounts others of little apparent consequence in the present discussion. All of these have been more or less affected by subsequent changes. Quartz has suffered least of all, the chief modification being a greater angularity of form and an occasional interlocking tendency caused by secondary growth [pl. 22, lower figure]. Both orthoclase and plagioclase feldspars occur. The orthoclase - grains, which originally made up more than half of the bulk of the coarser types of rock, have been in places profoundly altered [pl. 22, upper figure]. In many cases the identification of this mineral de- pends upon its association and the abundant remnants of character- istic structure and its normal secondary. products. In the least affected grains satisfactory identification is not difficult. “Even in the most modified representatives there is some preservation of structure indicating size of grain and proving the essentially gran- ular character of the rock. The plagioclase, although not abundant, is more readily detected than the orthoclase because it has been much less affected by the secondary changes. All original ferromagnesian constituents are wholly altered. There were some such constituents in the rock, as is plainly shown by the secondary products. Hornblende and biotite were probably both present. . | The secondary products, derived from the original feldspars and ferromagnesian constituents, include sericite, chlorite, calcite and Plate 22 Photomicrograph of bluestone, x 25 diameters. The clearer grains are quartz and indicate the approximate size of other original constituents. In this case the alteration of the feldspars and ferromagnesian originals is so complete that their products form an indeterminable complex agegre- gate of closely interlocked granules, flakes, and fibers of extremely fine texture. Photomicrograph of first grade medium grain bluestone, x 25 diameters. Taken to show angular and interlocking grains indicating secondary growth and a complete lack of reeding structure. The clear grains are quartz; the rest of the field is made up chiefly of secondary derivatives from the original feldspars and ferromagnesian minerals. GEOLOGY OF THE NEW YORK CITY AQUEDUCT I2!I quartz as the most important and abundant. Others probably occur that are less readily differentiated, and among them is kaolin. Occa- sionally a small amount of massive or granular pyrite occurs. There are traces of organic remains, especially plant stems, and the pyrite is most plentiful in association with those beds. It seems to be the secondary products largely that give the char- acteristic bluish or greenish color to this stone. Practically all of the iron freed by secondary changes from the ferromagnesian con- stituents has entered into new silicate compounds, especially with the chlorite, which are minutely distributed throughout the whole mass, giving it all a tinge of the characteristic color of these well known products. The same amount of iron in the oxid form would no doubt give as highly colored stone as any of the reds or browns of other familiar types of sandstone. But the tendency to form the sericite-chlorite-quartz aggregate in the rock has also an important bearing on its durability and strength. This is further discussed in a separate paragraph. Classification. It is clear that this type of bluestone is a sedi- mentary rock of medium grain, a sand rock or “renyte.” Since the silicates are so predominant in the original composition it may be further identified as a sandstone or a “ silicarenyte.” But in view of the predominance of the feldspars it should be further designated as an arkose sandstone. And considering the extent to which it has been modified by the development of interstitial sili- cious products and the effect that this has had in perfecting the bond between the grains, the rock may be classified as an indurated arkose sandstone. Special structure. A study of the cause of reeding, or the tendency to split into slabs, led to the preparation of thin sections of this structure [pl. 23, upper figure]. It is apparent from them that the reed is strictly a rock structure and that the perfection of the capacity to split along these planes depends wholly upon the abundance and arrangement and size of the elongate and semifibrous grains and the presence of a more than usual amount of original fine or flaky material. Almost universally the reed streaks are darker in color and finer in grain than the average of the rest of the rock. In part therefore it is an original character due to the assorting action of water during deposition, finer streaks alternating with coarser ones in accord with ordinary sedimentation processes. But, in addition to that, the subsequent changes that have affected the whole rock have occasionally accentuated the structure by a ten- . i 122 NEW YORK STATE MUSEUM dency of the whole rock to develop elongate or fibrous aggregates. | It is probable therefore that the parting capacity is in places con- siderably increased by the very process that has produced just the reverse results in the more heterogeneous portions of the beds. Under a sufficient stress the rock will part most easily along the — planes where this foliate or fibrous character is most persistent. Even in these cases, however, it may not indicate that the rock is essentially weak. It simply locates the most vulnerable point in the stone. In many quarries these streaks are so abundant that only thin slabs can be obtained —the disturbances of ordinary quarrying being sufficient to cause parting. The deeper portions of quarries are, however, much less subject to such behavior. In all cases the greater slab development of the exposed portion of the ledge is an ordinary weathering effect, by which the same results are obtained slowly and naturally and more perfectly than can be secured artificially on the fresh material of the same beds. The expansions and contractions of changes of temperature, together with the rupturing effects of freezing water caught in the pores, serve finally to weaken every part of the rock. In this process the prominent reed lines give way so much in advance of the rest of the rock that they develop into true rifts and separate slabs appear. It must be appreciated that these ledges have been exposed an 1m- mensely long time compared with the probable requirements of any engineering structure, and that this weathering tendency does not mean a speedy disintegration of the freshly quarried blocks. Still it is advisable to avoid as many sources of weakness as possibic and one of the ways is to select ledges where the stone does not have a reeding tendency, or in which the reed lines are interlocked, or wavy, or interrupted. These requirements are most fully met in the coarser beds and especially those exhibiting some cross-bedding. Two local quarries meet these demands to a marked degree. Strength. The better qualities of, bluestone have great strength. Even the reed lines are in many instances stronger and more durable than the regular quality of some other sandstones that are usually considered suitable building material. The secret of this exceptional strength lies in the modifications of texture that have resulted from the alteration and reconstruction of the mineral constituents. The breaking up of the orthoclase feldspar, and the accompanying changes in the ferromagnesian minerals, have fur- nished considerable secéndary quartz, which has in part attached to the original quartz grains making them more angular and de- Plate 23 Photomicrograph showing structure of the reeding quality of “blue- stone.” Magnification 30 diameters. Taken to show tendency to paral- lelism of elongate grains. Photomicrcgraph of best grade coarse-grained bluestone. Taken to show a quality in which the granular character is still well preserved. The clear grains are quartz, the others are chiefly feldspars somewhat modified. The close interlocking and the development of fibrous or frayed structure and the bending or wrapping of some constituents are secondary effects. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 123 veloping an interlocking tendency [pl. 22, lower figure]. At the same time the fibrous sericitic and chloritic aggregates have developed to such extent as to fill most of the remaining pores, and in many cases the fibrous extensions have actually grown partly around the adjacent quartz grains [pl. 23, lower figure]. The effect has been to develop a silicious binding of unusual toughness. This combina- tion of changes has made a rock that is now remarkably well bound or interlocked for a sedimentary type. Durability. First-class stone of the grades indicated above would have as great durability as any stone in the market, except perhaps a true quartzite. With the exception of the almost neg- lectable quantities of pyrite, occasionally found, there is no con- stituent prominently susceptible to decay. The rock as a whole mineralogically is stable and its texture indicates unusual resist- ance to ordinary disintegrating agencies. General conclusions From the microscopic study it is clear that the variety of rock most fully meeting the demands of heavy exposed construction are the coarser beds and those freest from reed and shale. From the field study it is apparent that ledges of suitable char- acter occur occasionally and that at least three such are not far from the Olive Bridge site. From additional explorations it is certain that ledges of high grade rock occur, and that the grade varies rapidly in the same bed and that suitable material can be obtained in the immediate vicinity of the Ashokan dam. No doubt rock of equally high quality may be obtained at many other localities. men eats CHARTER Vi THE RONDOUT VALLEY SECTION Because of the fact that the hydraulic grade of the Catskill aque- duct as it approaches the Rondout valley is nearly 500 feet A. T., an elevation more than 300 feet above-the lowest portions of the valley and more than 200 feet above very large areas of it, a total width of more than 4 miles being too low for unsupported con- struction of some kind, and because of the general policy of using the pressure tunnel system so as to deliver the water at a corre- sponding elevation on the east side of the valley, and further because of the very complicated geological features of the district this section has been the seat of very extensive and interesting explorations. Undoubtedly a greater number of obscure features occur here than on any other single section of the whole aqueduct line. Most of these features are readable from surface phenomena in general terms. In all cases the indications are plain enough to serve as a guide to well directed tests, but many points of critical importance can not be determined with sufficient detail and accuracy of posi- tion for such an engineering enterprise without systematic explora- tion.t The basis and results of this line of investigation which has occupied the greater part of two years are summarized and plotted in the following discussion and.charts. The portion receiving special study is in the vicinity of High Falls. General geology Almost everywhere the surface is glacial drift. Where outcrops of bed rock occur they habitually present the unsymmetrical ridge appearance usually with a more or less sharply marked escarpment on one side and a gentle slope on the other. The strike of these 1 These explorations belong to the Esopus division of the Northern Aqueduct Department. The earliest reconnaissance was done under the direction of James F. Sanborn, division engineer, who was subsequently assigned to geologic work over a con iderable portion of the Aqueduct line. The development of exhaustive explorations and final construction on this division has been carried on under Lazarus White, division engineer, assisted by Thomas H. Hogan. The division has been recognized from the beginning as an important one and in many ways one of the most com- plex. Thomas C. Brown, now professor of geology in Middlebury College, was employed for a year on this division during the later exploratory work. 125 126 NEW YORK STATE MUSEUM features is in general northeasterly and on the gentle slope is the westerly one. It is apparent at once that the valley bottom is a complex one and that its history has been somewhat obscured by the glacial deposits. Formations. The following distinct stratigraphic units are deter- minable in this valley every one of which will be cut by the tunnel beginning at the west side with the youngest formations: Feet Hamilios and Marcellas flags and.suales.- 4 re o-e etek eee 700-+ Onondaga littestone .. 026.4: : 102 ae ee ee ee ee oc eee ee 200 Esopus gritty’ shales. {0.9% bo. 3o5 se tee Se ee ole Saeco &00-+ Port Ewen shaley limestone including the Oriskany transition........ 250-+ Bectraft. crystalline Inmestome £)4 0... hte co eee ese oc ose meee 75 New Scotkind shaley. mestone: “-. 3-5-4 3 cee eee Cae aoe eee 100 Coeymans lamestone. 224.55. on os Se eee eee te eee 75 Manlius limestone including Rosendale, Cobleskill, and the cement bé@ds . 0.0.2. jc see ate Se es © ee +h Regedieetee 100-+ Binnewater sandstovéve go. <22,05 adh «ei oe eee ae oe dk Wes 50 High Falls shale including small Gace PRICES Bi ce ok ss Seemed 75 Shawangunk cong lomeiates: .s. aca ee oe eee ele kee 250 to 350 Hudson River slates —thickness unknown; probably. more than...... 2000 Approximately 4775 These occur in belts in succession more or less regularly from west to east. Most of the formations are quite uniform in the Rondout valley. The Shawangunk conglomerate is probably more variable than any other as shown by borings. Because of this general persistence of formation it is possible to estimate approxi- mately the depth at which any particular lower member lies if some starting point can be identified. [For detailed description of the formation, see pt 1] Structure. The principal irregularities are structural, rather than stratigraphic. The region on the west side of the valley, the margin of the Catskills, is but slightly disturbed and lies very flat, but the region on the east side, the Shawangunk mountain range and the cement district, has an extremely complicated structure. The Rondout valley, lying between them, is a transitional zone and passes from gentle dip slopes and folds in the westerly side to more frequent folds and thrust faults on the easterly side. In at least two thirds of the valley it would appear from surface evi- dence alone that the formations would dip uniformly westward, the only suspicion of additional complication being given by an occa- (Zo61 ‘“ABojlOs5 Ur [OOYIS JowIWINS AjistoAruy, eIquinjod Aq ydvis -0J0Yg) ‘Yoo1d JnopuoY Uo sey YSipY ye opeys sey YStpT puv ouojspurs so}eMouulg IY} UI Pjofy 1oUTM VY ~ v2 93e[d GEOLOGY OF THE NEW YORK CITY AQUEDUCT 127 sional minor fold seen in the river gorge or an escarpment where the sedimentary character alone would hardly account for it [see pl. 24, High Falls]. Explorations have shown that the evidence of the minor structures is reliable and that disturbances occur at some places even to the extreme western margin. Physiography. In spite of the drift cover which obscures many original inequalities it 1s readily seen that the prevalence of the gentle westerly dip over most of the area, together with the succession of so many different beds of varying resistance to ero- sion, have allowed the development of a succession of long dip slopes and steep escarpments on a more pronounced scale than the present topography shows. It is clear that the Rondout is really a series of these unsymmetrical valleys. The principal large dip slopes are formed by the Shawangunk conglomerate and the Onon- daga limestone. In each case an original stream had adjusted its course fully to the structure and was shifting slowly by the sapping process to the west against the opposing edges of the overlying strata which form the bordering escarpment. One of these unsym- metrical valleys lies along the easterly base of the Hamilton escarp- ment and is continuous with the lower course of Esopus creek farther to the north. In the area under special study it is not occupied by a stream now but is filled with glacial drift so com- pletely that the original stream has been evicted. It is evident, however, from computations based upon the average dip of the slope carried to the base of the escarpment that the bed rock floor ought to be from 200 to 300 feet below the present surface in the deepest portion. Borings have proven this to be the case both along the present line near Kripplebush and also on the first trial line across the Esopus at Hurley. The same thing is true near High Falls in the center of the valley where Shawangunk conglomerate forms the dip slope and the escarpment is formed by the Helderberg limestones. In this case the drift filling is very deep also, and Rondout creek flows upon it quite independent of rock structure except where it has cut across the margin as at High Falls. In the eastern half of the valley the hard Shawangunk conglom- erate forms the chief rock floor and largely controls the contour by its own foldings and other displacements. Thus the Coxing kill tributary valley lies in a syncline of the conglomerate with occa- sional remnants of overlying beds as outliers adding some variety to the form. The Shawangunk mountains, as a physiographic 128 NEW YORK STATE MUSEUM feature, owe their present elevation chiefly to the resistance of this conglomerate which serves as a protective member among the formations. On the west side, the foothills of the Catskills form a part of the cuesta developed by the erosion of Paleozoic sediments, the inface coinciding with the escarpment along the lower Esopus and Rondout valleys at this point. It is certain therefore that the drainage of the Rondout valley before the Ice age differed materially from the present lines. A stream, probably the original Rondout, followed near the western margin of the valley and joined the Esopus as it emerged from the Hamilton escarpment to turn northeast. Another which had cut somewhat deeper occupied the central portion of the valley and probably joined the Esopus at some point farther north — its lower course is not explored. Practical questions The chief practical questions to be given as full answers as pos- sible are: 1 At what depth must the aqueduct tunnel be placed in order to be everywhere in substantial bed rock with sufficient cover to be safe? 2 Where are the most critical places—those whose geologic characters are such as to demand exploration? And at the same time which sections may be safely left without testing? 3 What is the rock structure and condition? And are there rea- sons for believing that the tunnel plan is not feasible at this point. If so, where can a better one be found? 4 What is the character of underground circulation of water? 5 What formations will be cut at the different points and which should be favored or avoided wherever possible? From the fact that the present Rondout flows across solid ledges at High Falls and at Rosendale from 100 to 200 feet above the known rock floor of the preglacial gorge where explored it is clear that the present course is entirely different from the original. The Coxing kill, the third and most easterly of these streams is not so much disturbed although it also is shifted. It is worth noting that the streams of this valley together with the lower Esopus and the Wallkill river have become so completely adjusted to the rock structure that they all flow up the larger Hudson valley, of which all form a part, and join the master stream GEOLOGY OF THE NEW YORK CITY AQUEDUCT 129 at an obtuse instead of the usual acute angle. They are essentially retrograde streams. Explorations. Systematic explorations and tests are repre- sented chiefly by drill borings through drift into the rock floor. These were supplemented by two test tunnels for working character of material and a series of tests on the behavior of certain of the drill holes, together with other tests on material. The results are embodied in the accompanying cross sections and the additional discussion of special features. Detail of local sections Kripplebush section. This from the first was reearded as one of the critical sections because of the buried gorge along the base of the Hamilton escarpment and because of the doubt as to the behavior of the Onondaga limestone. On the accompanying section the borings are plotted and the structure as now interpreted is indicated. The dip slope formed by the Onondaga limestone is covered by 200 to 250 feet of drift, mostly modified drift. The strong valley character of the rock floor is almost wholly obscured by the glacial deposits and the present brook, an insignificant stream compared to the preglacial one, occupies a position above the escarp- ment instead of above the old channel. After a couple of the central holes were finished, it became appar- ent that the structure is not nearly so simple at this point as the general surface features would lead one to expect. It was clear that a simple dip such as was proven to prevail on the dip slope would not account for the much greater depth attained by it in. the vicinity of station 500. The discovery of this additional feature raised two questions: (1) Is the structure a flexure or is it a fault, and if a fault whether normal or thrust, and (2) what is the prob- able effect of this structure on the position and depth of the pre- ~ glacial gorge? The habit of the district immediately east of the valley would support the theory of a thrust fault. The nature of the immediate area would suggest a simple flexure while it is manifestly possible that a normal fault could easily occur. Later explorations! have 1Since the above was written the tunnel has been completed through the Kripplebush section. Although faulting is indicated by the borings and actual occurrence of the beds it is very difficult to find the fault. A part of the displacement is accomplished by the steepening of the dip but this will not account for more than half of it. 130 NEW YORK STATE MUSEUM F Tans ith: i TAY Fig. 19 Geologic cross section of Kripplebush section of the Rondout tunnel line as interpreted from drill borings GEOLOGY OF THE NEW YORK CITY AQUEDUCT ESE tested this zone so well that it is practically certain that the feature must be regarded as a fault of some type with a displacement of nearly 200 feet. The striking physiographic feature is the development and preservation of the escarpment on the downthrow side. This occurrence is certainly a very unusual case in that regard [see fig. 19]. Because of the intention to construct the tunnel deep enough in bed rock to reach safe rock conditions the question of depth of buried gorge becomes an important one. As soon as it was dis- covered that a fault existed there the problem became of sufficient prominence to demand more detailed exploration. If the faulting is accompanied by a broken zone in condition favorable to more ready erosion, it would be possible that the original stream in work- ing down this dip slope might become entrenched in the fault zone aad at that point begin to cut a narrow gorge instead of continuing the sapping process. In fact, it would undoubtedly do this very thing if there is such a crushed zone of any consequence and if the erosion process were allowed to continue long after reaching this critical point. As a matter of fact explorations have shown that there is a thin layer of Hamilton shales still remaining on the Onondaga and the deepest point found is on the Hamilton shales side. These facts in connection with the failure to find any deep notch indicate that there is probably no zone of much greater weakness than the shale member itself. It is reasonable to conclude that the rock floor can bé safely regarded as not much lower than 88 feet A. T. and that the rock condition is not especially bad for tunnel construction? even in the fault zone. | Rondout creek section. This is the central portion of the valley including the depression occupied by the present Rondout and the exposed edges of the series of shales and Helderberg lime- stone. The repetition of the dip slope and escarpment, together with the heavy drift filling and the occurrence of so many forma- tions together make this an important section. All formations from the Shawangunk conglomerate to the Port Ewen shaly limestone occur at this point, and although there is little outward evidence of disturbance it is certain that whatever difficulty is tc be found in this variable series is likely to be met here. It is therefore a sec- tion that requires exploration both for depth of preglacial channel and for quality of rock. 1 In construction this ground has proven to be good and sound throughout. 5 132 NEW YORK STATE MUSEUM WH), 4 Wi) ° 7 TENE It Esopus Shales any atest jail eee TH \\ CN NS 6/0 AN NINA ~ SURFACE PROFILE 250'X Fig. 20 Geologic detail of the central Rondout section constructed from exploratory borings data WEST EAST _ GEOLOGY OF THE NEW YORK CITY AQUEDUCT 133 All of the formations dip westward wherever exposed, but the dips vary somewhat, nearly all being of low angle. Occasional minor inequalities of the nature of small rolls may be seen, as, for example, the small fold in the gorge at High Falls [see pl. 24]. Explorations have shown, as indicated on the accompanying cross section [fig. 20], that there is a deeper buried gorge here than at Kripplebush. The deepest point discovered is a few feet below tide level. The escarpment is steep and is formed by the Coeymans and New Scotland formations. The dip slope is Shawangunk conglom- erate, High Falls shale and Binnewater sandstone, with the Manlius limestone forming the floor. Identification of the drill cores which penetrate the limestone indicate that the dip slope is reversed on the west side of the gorge and that the stream had really reached about the axis of the trough. A discrepancy in thicknesses and depths in hole no. 34 by which it appeared that the Coeymans formation was almost twice as thick as usual and that it contained a broken or crushed zone leads to the interpretation that there is a small thrust fault here which re- peats the formation as shown on the accompanying cross section. Instead of a uniform westerly dip of all formations from the Rondout westward it is proven that minor anticlinal rolls and even thrust faults, as in this case, or such faults as in the Kripplebush case are not to be excluded. This structural relation has a direct bearing upon the question of the thickness of the Esopus shales. The Esopus is certainly not so thick as would otherwise be supposed, by 200 or 300 feet at the least. The true thickness is still an unknown quantity (estimated at 800 feet). It is clear that the aqueduct tunnel will have to be constructed a considerable depth below sea level at this section, probably not less than minus 150 feet, even if the character of the formations be neglected. But the character or quality of these formations in view of their structural relation constitutes the chief problem. Because of the fact that every structure reaches the surface and eventually dips gently to the west in such manner as to encourage water circulation, their water-carrying capacity or general porosity becomes of great importance. A great capacity is all the more serious because of the heavy drift cover within the abandoned gorge, on top of which 1 This portion of the tunnel and its continuation south to the Shawangunk range has been constructed at 250 feet below sea level. 134 NEW YORK STATE MUSEUM the stream flows and which constitutes essentially an unlimited storage reservoir to feed underground circulation. This is all the more true if crush zones are extensively developed as accompani- ments of the faulting. In general as to perviousness the indications are somewhat ob- scure. But the data now obtained seem to prove that all the for- mations except the Binnewater sandstone and the High Falls shale are compact and fairly impervious along the bedding lines. - Only where crevices have formed or where crushing occurs is there likely to be heavy circulation. This is all the more important since so many of the beds are limestones known to be readily soluble in circulating water. One of these limestones, the Manlius, exhibits occasional large open solution joints at the surface — so large that a surface stream disappears entirely at the so called “ Pompey’s cave’ and joins the subterranean circulation. But such caves are probably limited to the surface. It is near this point, however, that one of the earlier borings at one side of the present line discovered very soft ground at a depth of about sea level, i. e. over 200 feet below the present surface, which shows that similar conditions prevail at certain points to great depth. Pumping tests made on hole no. 32 in an attempt to establish some data on the inflow of water gave very interesting results. These tests were very thorough. It was proven that the water was supplied in apparently inexhaustible quantity at maximum pumping capacity, which was ninety gallons per minute. Futhermore, the chief inflow seemed to be from the Binnewater and High Falls formations as was to be expected. Whether a crush zone allowing free circulation is furnishing a portion of this supply or whether the whole inflow represents the normal porosity condition of these formations is not yet proven.* Other porosity tests have been made in such way as to locate and measure this factor [see later discussion]. Hole no. 10 shows an artesian overflow that comes from the Binnewater sandstone. A working shaft has been put down also in the vicinity of hole no. 32 and at the same depth found an enormous inflow of water which drowned out operations for a time. The lateral supply in this case has been reduced by introducing a thin cement grouting through holes bored in the surrounding rock irom the surface. Holes no. 12 and no. 14 also show an artesian flow, but both are 1 In construction the Binnewater sandstone has been found very wet. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 135 shallow holes and the supply comes from near the contact between High Falls shale and Shawangunk conglomerate. It 1s certain from these observations and tests therefore that the Binnewater sandstone and High Falls shale are more porous than the other formations, and because of the serious difficulties arising from so heavy inflow of water from them the tunnel grade should be shifted so as to avoid these formations as much as possible. A comparison of the accompanying cross section, which is drawn to scale [fig. 20], will show that a tunnel on one level would neces- sarily run for a long distance in these beds because of the gentle syncline. Furthermore, they lie at about the depth that would otherwise be a safe depth below the buried gorge. But a tunnel with a step-down, i. e. one run at two different levels could avoid most of this poor ground. By approaching at a level of about — 50 feet or — 100 feet in the limestone beds to station 600 (hole no. 34), then stepping down to — 250 feet, the line in a very short distance crosses these two porous formations and enters the Shawangunk conglomerate which is more substantial, and, all things considered, one that seems most advantageous for successful construction. It will have to maintain a head of more than 7oo feet as the difference between hydraulic grade and the tunnel level in this section. Under these conditions rock quality and condition are of greatest impor- tance and there is no doubt about the advisability of avoiding the poorest formations in some such manner. | Coxing kill section. On the line of exploration the Coxing kill flows over Shawangunk conglomerate and. High Falls shale. Both dip plainly eastward, and a hole no. 11 located on the east side of the brook penetrates about 70 feet of drift and shale. But only a hundred feet to the east Shawangunk conglomerate outcrops at the surface dipping the same way. It is certain therefore that a fault occurs here. The dip of the fault plane is indeterminate from the surface, but the relations and surroundings indicate a fault of the thrust type. Later explorations indicate that the fault plane is rather flat [see cross section fig. 21] so that the shales are repeated above and below a tongue of conglomerate. Boring no. 11 has also an artesian flow of considerable volume coming from near the bottom of the conglomerate. It is a mineral water. | The chief importance of this section as a problem in applied geology lies in the influence of the fault and the maximum de- pression of the conglomerate. If the tunnel, which enters Hud- son River slates at the Rondout creek section at — 250 feet can be kept within that formation throughout the rest of its course, 136 NEW YORK STATE MUSEUM there is no doubt that an advantage will be gained both in the greater imperviousness of the rock and the greater case of pene- tration. Wherever the conglomerate is undisturbed it is perfectly good, but where broken the crevices are but imperfectly healed and circulation is unhindered. It would therefore be desirable to know whether at — 250 feet the whole of the downward wedge of Shawangunk could be avoided. The borings indicate a thickness of Shawangunk of 345 feet in hole no. 11 where it is cut at a small angle, and a thickness of 409 feet in hole no. 36 where it prob- ably lies pretty flat. This greater thickness together with the LLEELEZEZETXEZ’ Yj. a Ze Se LiL = 3 sooolt. Fig. 2x Structural geologic detail of the Coxing kill section finding of crushed rock at about the — 100 foot level leads to the conclusion that the formation is overthickened here by the thrust fault to the extent probably of about 75 feet. The true thick- ness of the formation at this point is doubtless more nearly 300 feet than either of the figures obtained directly from the two holes. If this interpretation is used as the basis of plotting a cross section [see accompanying cross section] it is apparent that the conglomerate should not be expected to extend more than a few hundred feet east of hole no. 36 and it probably does not reach a much greater depth than the — 236 feet represented as its base in that boring. 1 Construction of the tunnel has progressed far enough through this sec- tion to prove that the Shawangunk formation does not reach much lower. It forms the roof of the tunnel for some considerable distance but does not come down into the tunnel more than a foot or two. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 137 Shawangunk overthrust. At the extreme eastern side of the Rondout valley near the point where the surface reaches hydraulic grade again, the surface outcrops pass from High Falls shale to Shawangunk conglomerate to Hudson River shale in the normal order but with entirely too small an area of conglomerate consid- ering the character of the formations. The higher ground is all Hudson River in the vicinity, and there is abundant evidence of crushing and disturbance. It is evident that a thrust fault is again encountered here, one of sufficient throw to bring the Hudson River slates above the Shawangunk conglomerate — probably a lateral displacement of very great extent. Explorations have fully proven the existence of this fault. The accompanying diagram shows a cross section as now outlined by complete penetration of two borings. Two trial tunnels were run to test working quality of Hudson River slates compared to Shawangunk conglomerate at this locality. Both are within the influence of the fault zone. Both are there- fore more broken than the normal with the result that the Hudson River slates probably show poorer condition than usual and more troublesome working, while Shawangunk conglomerate probably shows easier working than usual. It is believed that normally the two rocks would present a greater difference than was found in this test. Special features Several questions, some of which have a practical bearing, have been raised as separate features during the exploration of the Rondout valley. Caves. One of these is in regard to the possible existence of underground caverns. This was given a special prominence early in the work by the experience of one of the drills. After pene- trating the limestone series near High Falls to a depth of over 200 feet, the drill seemed to leave the rock and enter a space allowing the rods to drop 28 feet before being arrested by sclid material. The further attempt to work in this hole resulted in the breaking of the rod down at this point and the subsequent failure to recover the diamond bit which is still in the bottom of the hole. The question is as to the meaning of this occurrence. Is it a cavern? “Pompey’s cave”’ has been referred to in an earlier paragraph. This is clearly not much of a cave. It is essentially an enlarged joint or series of joints by solution along the bed of a surface 138 NEW YORK STATE MUSEUM stream to such extent that the stream normally at present has be- come subterranean. It is the writer’s opinion that the case en- countered by the drill boring is similar. The apparent cavern is probably a slightly enlarged joint along a line of somewhat abun- dant underground circulation and perhaps associated with some crush zone developed by the small faulting known to occur in this immediate vicinity. .It is probably not entirely empty but contains residuary clay, and in all likelihood is very narrow and not exactly vertical, so that the drill rods were bent out of their normal course and wedged into the lower part of the crevice. Smaller spaces of this sort were encountered at a few other points.2 These occurrences seem to indicate that the limestone beds yield rather readily to solution by underground water, and that this cir- culation has been at one time active to at least 50 feet below pres- ent sea level. With present ground water level nearly 200 feet above sea level it is extremely unlikely that any such action is going on at so great depth. The occurrence is therefore strongly corroborative of former greater continental elevation when the deep stream gorges, now buried, were being made. These deeper caverns or solution joints probably date from that epoch. Imperviousness and insolubility. The question of impervious- ness and closely associated with it that of solubility, is of great practical importance in this particular work. The immense pres- sure under which the tunnel will be placed in crossing this valley makes it impossible to construct a water-tight lining. Everywhere much depends upon the rock walls to help hold the water from serious joss. Wherever the-rock is fairly impervious except occasional crevices or joints they can be grouted and safeguarded satisfactorily. But where a formation is of general porosity this can not be so successfully done. Even more difficult to handle ts the rock wall which is soluble and which therefore with enforced seepage may tend to become progressively more porous. That this consideration is not wholly theoretical is shown very forcibly by the Thirlmere aqueduct of the Manchester (England) Waterworks. In that case a 3 mile section was built through limestone country using the same local limestone for concrete aggregate. Although 1JIn constructing the tunnel several clay-filled spaces have been discovered in the same vicinity at elevation—1o0. One of these extended vertically with a width of I to 2 feet and from it a great mass of mud ran into the tunnel. At one point it was connected with a horizontal space of the same kind extending 15 feet. It can be seen that the original crevices have been en- larged by water and that they were originally formed during faulting. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 139 this concrete was mixed as rich as I part cement to 5 parts aggre- gate and the work was well done, excessive leakage reaching a total of 1,250,000 imperial gallons per day was developed within a year. It was found that the limestone fragments of the aggregate were corroded forming holes through the lining of the aqueduct and that these holes actually enlarged outward. All this was done under cut and cover conditions with not more than a 6 or 7 foot head on the bottom of the aqueduct. In the Rondout valley, the aqueduct will cut no less than 6 lime- stone beds in all cases under great pressure. This fact will in all probability tend to increase the action. But, of course, some of the beds may not yield so readily to solution. Tests made thus far, however, indicate that all are attacked in water. Considering these facts it seems desirable, so far as possible, to avoid the limestone beds wherever rock of greater resistance to solution can be reached, and further it is equally desirable to use a more resistant rock for the lining concrete. So long, however, as the formation is not very pervious so that a new circulation could not be established by the escaping water there would be little harmful effect. An average of five analyses of the Thirlmere limestone, different varieties of the same formation, gives the following: See iru SIcIMISKIATLETAR ue ae Lek RE RE IE ee 2.77270 Puiiaiiia sand Irom oxi AlsOstPesOs. 12205 oak oc che ce eee odes 0.276 1a EE Seg OVE TE Ge re RU URE es a en se 53.076 TA SURES TODAY EL ORE Pe nO a Se ea a ee a . 390 RMR BTM uCHOUIV CLE Tells Caer aytice ar wick hi Bic dacs Sicle yea alee 6 6 Ep aA es 42.248 LEE Sil is ae SS il a ann LRA : Lihat para F t 1 i 7 i 7 . i + : - Ps a £ AG A ; ; wh 7 7 BP i : teal Ks :) . le Ae > Stace a. - - mS ss \ / ¥ qi j ign ' 7 ‘ ‘at “aol ae 9 oe P. % © ‘- ; pg i ¥ i r iy te wy ad Wy iy i or ae it r a 7 Me I ai + Hane A hich Ys ! 2 ae eee is " ye | [uUN; Sinsseid ynopuoy 247 uo s8uLI0q AuOyEIO]dxo UL perndas BEp ty Wosy poyzonsysu0-) ont 95 $5019 aRO]OIy zz “iy volp SACLT eos ArtErenlimestene nd 2 ri Cerskanylimes/ird feacrat Limestehe 4 Wer Zeatland & d 3 Ymestone ~ Qoeyrmans Limestone \ 3 Martius Limestone Diane rater Jandstone & 5 ADEA InOpuoyY ay) Jo uoN>: “Gh Falls Shale & 3 8 oS 8 8 Hi YG |e H7- 2 MEF Hays. toN ESCARPMENT NEAR HRIPPLEBUSH ppnwete reek or v7, ee BURIED GORGE Road or PRECLACIAL STREAM ee ke wa eo wo lazSo Broek bn. Wo CRUSH ZONE - 12. loa b.o%e 4219 Fenn e. Laoter 353 BveleD GORGE lane Ce = FRECLACIALITREAM pai- 1029 O09 1299 Lysis do hy AS £8 TTS nS) (aE Q lets dt 6 abate ° si Yo ad ip Ss F Syies ef fe = may. | fe fy a ae 5 Wigs ile is 3 SIE CS Sic VN cn aE R ny 7 ore Q | fe 3 S Fondout Creek b.o% Road lno7« Kanal nbupH bye ane Break Koad In 220 loxinng Ki ; ~ a Matoe Bie is ’ 1 ’ Rr ris Dw 4 won ywowsgenn Fo Cy Cine Say ‘a ae ee ex SONY ws | ~ oBWBLED GOBeg MANA AGL GEOLOGY OF THE NEW YORK CITY AQUEDUCT 14! Rondout siphon statistics 1 Total borings on the sipkon line. Three different boring equipments have been used owned by different parties and records have been kept so that the work of each can be followed or com- pared with the others. On this division the Board of Water Supply owned and operated one machine with their own men, another equipment was owned and operated by C. H. McCarthy, while a third which finally did a majority of the work, belonged to Sprague & Henwood, Con- tractors, of Scranton, Pa. The totals of different general types of material penetrated by these machines are as follows: Feet Feet Total Per cent ot of feet of of core drift rock depth saved Gee Wier on auipimente-cgan. “ni. octat os 1740.5" 2I75. 5 3016 89.4 Gropracic. & Henwood! is. ....2022 5.660. 3047 6831 10478 60.04 mereCarthy machine 2 oF 6) OS ee es 181 1228 1409 78.1 The average saving of core by all machines, cutting all kinds of bed rock was 75.96% 2 Core recovery from various strata. So nearly as can be done the strata represented in the drill cores have been identified and summarized as to total penetration and core saving. The core saving is a factor of prime importance in judging of the quality of rock and its freedom from disturbance. The following items are gathered from a study of the whole series. a@ Holes 6, 10, 12, 13, 15, 17, 18, 21, 22 and 25 penetrate Helder- berg limestone, a total combined depth of 1096 feet. Individual holes vary in core saving from 39.3% (no. 13) to 95.3% (no. I5). The average core saving is 78.19%. b Holes 8 and 9 are in Onondaga limestone with a total pene- tration of 197 feet. The core saving varies from 56.2% to 92.8% with an average of 74.5%. c Holes 11, 19, 20, 23, 24, 27 penetrate Hudson River shale and together represent a total of 696.5 feet. The core saving varies from 16.6% to 89%, with an average of 42.14. @ loles,6, 10, 11, 12, 14, 16 and 20 cut High Falls shales to a combined total of 410 feet. The saving varies in different holes from 17% to 83.3%, with an average core saving of 44.54. e Holes 8 and 26 penetrate Esopus shale and penetrate 76 feet. 142 NEW YORK STATE MUSEUM The core saving varies from 73% to 84.6¢, making an average of 78.8%. f Holes 10, 11, 12, 14, 16, 19, 20, 23, 24 and 27 penetrate Shawan- gunk conglomerate a total of 1356.5 feet. Core saving varies in different holes from 33.3% to 100%. The average recovery is 60.524. g Holes 6, 10, 12, 15 and 16 cut Binnewater sandstone. The total penetration is 205 feet. The range of core saving is from 30.6% to 74.7%, with an average of 562. h Holes 7 and 9 cut Hamilton shales to a total amount of 65 feet. The range of saving is 70% to 81.8%, with an average of 75.9%. 3 Artesian flows. Several of the borings struck artesian fiow of water. The fact that the sources of this flow are not the same has led to a tabulation of these data. RECORD OF ARTESIAN FLOWS Flow ; Static Flow encountered Hole Size in head gallons at elevation mo. inches infeet Minute Day Feet Strata IO I 18 30 43 200 —I09 ....Binnewater sandstone II I 10 10 14 400 — 60 ....Shawangunk conglomerate 12 3g I «Fee eee nase — 24 ....High Falls shales 14 TA BAL se A, eee + go : * 20 3% 7G IO 14 400 +108 ....Shawangunk conglomerate 23 2S ae ee wibnatt Ma Nae eet ee ne ‘ 31 DME kt coed RE Sas PAE Fs = 1s a hey Ano v3 39 aaa fcr he EES wha MSA hp +112 ....Helderberg limestone SNE xK 7 ee 432 +203 ....Hamilton shale (possibly drift) Pumping experiments and porosity tests Systematic tests have been made for flow of water, behavior of ground water and porosity of rock on certain of the Rondout ex- ploratory holes under the direction of Mr L. White, division engi- neer. A summary of these tests has been furnished by him from which is quoted the following: In addition to determining the location and thickness of the beds and the general character and condition of the rock from inspection of the cores, serious attempts were made to determine the relative porosity and water-bearing quality of the rocks encountered for the following reasons. (1) To determine the probable leakage from the siphon when in operation. (2) To determine the probable amount of water to be handled in construction. These experiments were divided into three classes: (1) Observation of flow from cer- CEOLOGY OF aE NEW: YORK CITy AQUEDUCT I43 tain drill holes which showed sustained flow of water. (2) Pres- sure tests in which water was pumped into holes which had been sealed off and pressure and leakage noted. (3) Pumping tests in which water was pumped from 4 inch drill holes by means of deep well pump of the type used in oil wells, and fall of ground water during pumping and subsequent rise after cessation of pumping noted. A description of the first two and the results obtained from them follows: A substantial flow of water was observed from the following holes: 11/17: 50 gallons per minute through 2% inch pipe, static head 10 feet 10/17: 30 gallons per minute through 1% inch pipe, static head di FCCE 20/17: Io gallons per minute through 3 inch pipe, static head ge, fcc The static head was observed by adding on lengths of pipe until the water ceased to flow over. It will be noticed in the case of hole no. 10 that the flow from the 1% inch pipe is not that due to static head of 18 feet, but that due to a head of only % foot. In other words the friction head is about 17.5 feet, and the velocity head only % foot. This same condition holds true of the other holes from which a flow was obtained. This would seem to indicate that the amount of water is not very great but that it is under con- siderable pressure. It is believed that this pressure is caused by gas. A slight flow was observed from the following holes: 12/17, 14/17, 23/17, 31/44, 39/22, and 5/NE. The flow from most of these holes has ceased since the pipe used in boring was withdrawn. There is still some flow from the follow- mae holes: 11/17, 20/17, 25/17 and 5/NE. The flow from hole 11/17 is constant at about 10 gallons per minute. The others are too small to be measured. It will be noted that the only substantial flows encountered were from the High Falls shale, Binnewater sandstone and Shawangunk grit, and that it was possible to force water into these rocks in greater quantities and at a less pressure than in the other shales and limestones. Porosity tests. The method of making these tests was as follows: Wash pipe equipped with a device for sealing the hole was lowered to the desired elevation. The seal consisted of alternate layers of rubber and wood around the pipe preventing the water from escaping between the walls of the hole and the pipe. Water was then pumped in and pressure and leakage noted. The result of the pressure tests was to show in a general way: (1) That the pressure increased with the depth of seal. (2) That the leakage decreased with the depth of seal. (3) The maximum pressure in the grit was 140 pounds to the square inch and minimum 144 NEW YORK STATE MUSEUM leakage was 5 gallons per minute. (4) In the Hamilton shales a pressure of 300 pounds to the square inch with very little leakage was obtained. The unknown factors are too many and too great to make any reliable deductions from these experiments. | DATE APR./IO 1S ° } oer ORIGINA eed WATER _LE eae : NOTE— FEB.Z29-MAR27] PUMPED 490.000 GAL PROBABLE LIEVEL APR. O. aad SS NO. -SURF. EL. 260". Or K 2 ° ¢ 0 Zz ° a w a J J z 4 a < 3 ° Fr L Fr a B. r) Fig.723 Curve showing fall of ground water level while pumping;from_boring 34 Pumping experiments were carried on in holes 32/22 as follows: The apparatus used was a deep well pump of the type used in oil wells. The holes were of an inside diameter of 414 inches and were cased to the bottom. A 3% inch working barrel was then lowered to the bottom of a line of wooden sucker rods. The stroke was 44 inches and the nominal capacity of pump at. 38 strokes per minute was 60 gallons per minute or 86,400 gallons per day. The power was obtained from a 40 horsepower boiler and 35 horse- power engine belted to a 10 foot band wheel which was connected to a 26 foot walking beam. In hole 32/22 at station 607 + 50 the average discharge at 38 strokes per minute was go gallons per minute or 129,600 per day. The experiment was continued for 15 days and the total amount of water pumped was 1,071,000 gallons. The ground water level was not lowered. It will be noticed that the discharge at this point was 50% in excess of the theoretical capacity of the pump. This was caused by the presence of gas, the effect of which seemed to be increased by the churning action of the pump. This may also explain the failure to lower the ground water. The experiment at hole 34/22 was similar in character. The upper 230 feet of this hole had an interior diameter of 474 inches GEOLOGY OF THE NEW YORK CITY AQUEDUCT 145 and the bottom 274 feet a diameter of only 3% inches. At first a 2% inch working barrel was used to pump from the bottom and a discharge at 32 strokes per minute averaged 24 gallons per minute or 34,500 gallons per day. This was continued for about 15 days and the total quantity pumped was 490,000 gailons. The ground water level was lowered 17 feet at hole 34 and 4 feet at hole 32, 750 feet away. The 2% inch pump was then let down to a depth of 200 feet with a 234 inch casing reaching down to the Binnewater sandstone, depth of 437 feet. The average discharge at about 40 strokes per minute was 60-65 gallons per minute, or an average of 90,000 gal- lons per day. It will be noted that the discharge was much smaller than at hole 32 owing to the absence of gas. Pumping with a 3%4 inch pump was continued 16 days and 1,532,000 gallons of —— JAERI 27,1908. 4|P.my. _-_—_—— —_ Fig. 24 Diagram showing successive stages of ground water level between holes 32 and 34 during pumping water were pumped in addition to the 490,000 gallons from the 2%4 inch pump. The ground water level in hole 34 was lowered 36 feet in addition to the 17 feet by the 214 inch pump, but rose g feet in 26 minutes, and 30.5 feet in the next five days. In the next 22 days it rose 9.15 feet, or .42 feet per day. Reduced water level in hole 32, 750 feet away by pumping in 34, 15 feet, or 1 foot for each 120,000 gallons pumped. In the first MUSEUM NEW YORK STATE 146 t€ sjoy — Surduind 419372 —Joyem pPpuNnoIs JO S11 JO o}e1 BUIMOYS 2AIND 3A31 UBLVM ANNOYS WWNISIBO MoO1dG 1334 NI HLidsd Go Sati GEOLOGY OF THE NEW YORK. CITY AQUEDUCT 147 three days after pumping ceased water rose 5.2 feet, and in 22 days rose 9.8 feet or at the rate of 0.45 feet per day. During construction! shaft 4 located at same point as hole 32/22, station 607+ 50, has proved a very wet shaft, the inflow varying from 400 to 850 gallons per minute. Pumping at this shaft has lowered the general water level and correspondingly lowered the water level in hole 34/22 at station 600 + 00. ee ren ——4 HOLE 34 SS ees ’ ei ey {het pecctansy eS = Nore © =/READINGS JN HOLE en B > [READINGS IN HOLE 944, y all ee ee pares even Ho 34. JAN. [i908 oT 32 JAN. ao aa Fig. 26 Curve showing rise of water in holes 32 and 34 after pumping ceased in hole 34 u te] 3 M @ > | ” 3 ° a a oO r w uJ uu Zz zr EF a b r) 1 From this shaft after reaching tunnel grade,— 250 feet, and after running northward into the fault zone and porous shales, the contractors are pumping 1300 gallons per minute. vy, » te Ti etchsas ky a} fare j a f a Mares — <<. pes ». i P| 7 tig 27269 257 wei wad W158 UA 7193 DY D+F Was HYDRAULIC Tso), SURFACE ati alley RR Mine MMM TM Pi MW Ms Lif HALLAILL RIVER y by UU Moosen Kivex Kares + + MILLA Mi wid yy l y} % Sea evel Hupson River Staras Fig. 27 Profile and geologic cross section of the Wallkill valley from the Shawangunk mountain range to the hilly divide near Ireland Corners on the east side of the valley. dapted from drawings of the Board of Water Supply) The exploratory borings are represented, there ik an attempt to classify the drift variety, and the approximate position of the presture tunnel to be conirucied for the Catskill aqueduct is indicated — eh) A ee ae suck mok CHAP TP lat THE WALLKILL VALLEY SECTION Between the Rondout and Wallkill valieys the aqueduct is to follow a tunnel at hydraulic grade which so far as can be seen will cut only Shawangunk conglomerate and Hudson River slates. No doubt there are many complicated small structures which because of the nature of the slates can not be reconstructed. The work of tunneling is not advanced far enough to add anything. But in the Wallkill valley, where it is necessary again to plan a pressure tunnel several hundred feet below grade, a considerable amount of exploration has been carried on.t . These explorations [see sketch map fig. 8] are distributed along several lines crossing the valley at intervals between Springtown, about 3 miles north of New Paltz, and Libertyville, which is about an equal distance south. The geology is simple. Only Hudson River slates form the rock floor, and so far as can be judged no other formation is likely to be cut by the tunnels. There are no doubt many complicated struc- tures, both folds and faults, as indicated by the high dips, but again because of the nature of this rock it is impossible to discriminate closely enough between different beds to determine exact relations. The point of greatest practical importance lies in the fact that the rock is fairly uniform and, although much disturbed is of such nature that crevices and joints or fault zones are almost as impervious as the undisturbed rock. This is because of the tend- ency of a formation of this composition to heal itself with fine, compact clay gouge. In fact, the mechanical disturbance produces or develops the cement filling contemporaneously with the move- ment. It is chiefly a mechanical filling, whereas the healing of a harder and more brittle rock like a granite or a limestone requires more chemical assistance. An additional practical question involves the estimate of depth required to avoid any possible buried Prepleistocene gorges and maintain a safe cover to guard against undue leakage or rupture. 1Explorations on the Wallkill division are carried on under the direction of Lawrence C. Brink, division engineer. The final construction is in charge of James F. Sanborn, division engineer, with headquarters at New Paltz, N.Y. . 149 ca es 150 NEW YORK STATE MUSEUM To this end most of the explorations were made. Two lines less than a mile apart on which a few exploratory borings were made near Springtown indicate two buried channels, a master channel and a tributary from the west which converge northward. A maximum depth reaching 70 feet below sea level was found on the more northerly line almost directly beneath the present stream channel which flows on drift at an elevation of 150 above tide. The more southerly profile reaches only sea level indicating a gradient for the preglacial stream at this immediate locality of more than 79 feet per mile. In the vicinity of Libertyville, 5 to 6 miles farther south, where the aqueduct was finally located, the profile was found to be con- siderably higher. Intermediate profiles are shown in accompany- ing figures. The deepest point yet found on the Libertyville line is 65 feet above sea level. It is worth noting that the gradient of the ancient Wallkill is therefore shown to be decidedly unsymmet- rical. The rock floor formation remains the same although it may vary somewhat in character. Under these circumstances, however, - a gradient of 13 feet per mile from Libertyville to Springtown forms a sharp contrast with the 79 feet per mile represented at the Springtown locality. In view of the remarkable inorease of gradient and the narrower form it seems reasonable to regard this as a rejuvenation feature developed at the time of extreme con- tinental elevation. How much deeper the lower Wallkill may be, including the so called Rondout river, which is really a continuation of the ancient Wallkill and geologically belongs to this drainage line instead of to the Rondout, no one can tell. But it is at least interesting to observe that the intervening distance from Springtown to the Hud- son at Kingston is approximately 12 miles and that a gradient for that distance equal to the average known in the 6 miles explored, i. e. 24 feet per mile, would depress the outlet 288 feet more. That would be equivalent to 367 feet below sea level. If, how- ever, a steep gradient such as that at Springtown prevails in this lower portion it is necessarily much lower— for example if a 79 foot gradient is maintained it would be possible to reach a final outlet at —1029 feet. It is likely that an intermediate value 1s more nearly correct. This has, however, an important bearing upon the question of maximum Hudson river depth, especially the existence of an inner deeper gorge above the Highlands. So far as this Wallkill profile goes, it supports the gorge theory. It is certain that the Prepleistocene Wallkill flowed north not very dif- (AJddng J91e jo pivog Aq ydeisojoyqg) ‘esurt ureyunoU yUNnSsUeMEeYS IY} UL BeIDQ NOdUOIG PieMO} SUTYOO] AD]RA T[PFIeEM AL SZ 93e1d Plate 25 NO. AQUE. DEPT. B.WS. NYE. WALLMILL DIV. PROFILE SHOWING WASH AND CORE BORINGS LINE A - SPRINGTOWN i & . ~ z “ J © > > = —_— 2 ¥ een 8 Ss 8 Sees S = oy = 3 Q ~ = ~ < Siow i SS ~ a N“ y -y 8 ¥ ee x S S SN Q s N ; SoS SWS 5 3 S > 3 = $ S Sih aS S Seas CVS y S N ; : s 2 = ra SS Ss S = te n PS = nee aR Sare Westie eo ee = % és S Sas = tS N \ aa = ~ SoA ess aes Beers Ree Bee ee eek x LS > > ast = © ~ S as ee . XS = ee = ss > = 3 5 2 2 RN BOR ¥ RF : > oe ———__ gs y << 4S BS Py & ~ 2 NOS Aon sn Q S$ ee “ SiR Sis SR ek SS Nek ee ee RG Roe NS caste 5 ae ee eS DSESGN x = ROD Do SS Be, ie ea etee SS he 2 AO Res ek Se Ne ; W tases niwiiscerdh 9p a SS Ss CS SS Ss XS 8S = 8 SS Se Ss LS ee ae Ay eee . Pe Ss Shee = ~ = tS NR Gyr “: = 2a 2 pry “3 ee Sey g < Q S S x Nae S = 8 = xa a ee Ser 220 : . ah = = Ye S LS I ae aah 5 es : : aa i a, 3 j . 2 oe i Sevico fie, 20 { ' ase H iat i ? er) j . i i f= | Z ee WALLKILL SiPHON Se i z } i i i é ou =k ioe = oe s ‘ai ees | Profiles of the present and preglacial Wallkill channels near Liberty- ville, and a diagrammatic section showing the different types of drift-filling together with the borings which furnished the data GEOLOGY OF THE NEW YORK CITY AQUEDUCT I5i ferently from the present stream except on a steeper gradient, but in all probability the headwater supplies between this stream and the Moodna have been somewhat shifted. It is possible that some former Moodna drainage area is now tributary to the Wallkill. But these changes were wholly glacial in origin and the extent of such shift is indeterminate at present. It is a notable fact that a large proportion of the work of ex- ploration in this valley was done successfully by the wash rig. The extensive lot of data was gathered without much delay or difficulty. This is because of the nature and origin of the drift cover. A considerable proportion of the drift mantle especially in central and deeper portion of the valley is modified assorted sands, gravels and silts or muds. In part they represent deposits in standing water laid down at a time when the lower (north) end of the valley was obstructed by ice and while waste was poured into the valley from neighboring ice fields. It is impossible to reconstruct the beds of these materials with any degree of accuracy. But it is at least certain that lens or wedgelike layers of differ- ent quality of material were penetrated, indicating oscillation and overlapping of deposition conditions, boulder beds and till being interlocked with assorted sands and gravels. But there is appar- ently no evidence of ice deposits of greatly differing age. The accompanying profile and cross section is a representation of ma- terials on the Libertyville line based upon identifications made by the inspector of the Board of Water Supply of the Wallkill Divi- sion under Mr L. C. Brink, division engineer. CHAPTER VIII ANCIENT MOODNA VALLEY Moodna creek enters the Hudson from the west between Corn- wall and Newburgh not more than a mile north of the entrance to the Highlands. It is a retrograde stream in its backward flow similar to the Wallkill. But its channel at present is almost wholly on glacial drift which it has trenched to a depth of more than 100 feet below the average adjacent surface. How much of its retrograde course therefore may be postglacial is not so clear. It seems necessary, however, to account for all drainage on the north margin of the Highlands by streams flowing to the Hudson northward. There is no notch low enough for their escape elsewhere. The ancient Moodna must have carried most of this run-off from the district occupying the angle between the Wall- kill and the Highlands. This stream may have drained even more of the region now forming the divide with the Wallkill than does the present Moodna. In any case it must have been a stream of considerable size, capable of excavating a valley or gorge of greater prominence during the period of early Pleistocene rejuvena- tion than now appears. Furthermore its position makes it highly probable that tributaries of fair size entering in its lower course were also effective enough to require consideration. This conclu- sion has led to the exploration of the Moodna valley in consider- able detail in preparation for the aqueduct work. The Catskill aqueduct is to cross the stream near Firth Cliffe, which lies almost directly west of Cornwal!-on-Hudson, and be- cause of the low surface elevation across this valley, as in the others, a pressure tunnel in rock is judged to be the most suitable type of structure. The accompanying sketch map shows the location. | Explorations were conducted especially for the buried channels and character of rock floor. Geologic features The region is one of chiefly Hudson River slate. But there are inliers of the older rocks such as Snake hill which belongs to a long ridge of Precambric gneiss and granite, brought to the sur- face by folding and faulting and there are more rarely outliers of younger formations such as Skunnemunk mountain. Farther north [53 154 NEW YORK STATE MUSEUM at Newburgh a gneiss ridge is accompanied by limestone, but in its southerly extension the slates are in direct contact. This relation is believed to be wholly due to faulting on both limbs of the anti- clines. This gneiss ridge disappears southward beneath the drift, but the borings have shown that it continues across the aqueduct line, although it has lost its influence on the topography. There are other inliers of similar character such as Cronomer hill 3 miles northwest of Newburgh. Between these two gneiss ridges lies the southerly extension of the Wappinger limestone belt. But so far as is known it disappears beneath the Hudson River series long before reaching the line of exploration. Near Idlewild station, filling the space between the two branches of the Erie Railroad, there is a syncline containing the series of Siluric and Devonic strata which spreads southwestward to include Skunnemunk mountain, an outlier of Devonic strata. This is the only occurrence of these formations in this region south of the Rondout valley. The structure and stratigraphic features of this occurrence have been worked out by Hartnagel. Its northward extension in all probability terminates abruptly by a cross fault not far north of the Ontario and Western Railroad. From these occurrences southward to the Highlands proper nearly everything to be seen through the drift is Hudson River slates. The Highland gneisses are bounded on the north side by a fault or series of faults. This brings various members of the overlying series into contact along the margin. In the best place where a direct observation can be made the gneisses are thrust over upon the Hudson River slates along a plane that dips about 40 degrees to the northeast. It is probable that a displacement of as much as 2000 feet or more could reasonably be assumed at this place. The contact zone also is much crushed and bears every evidence of having undergone extensive disturbance of this kind. Others of this same type occur within the gneisses where weaknesses formed in this way permit the development of such notches as Pagenstechers gorge. In some cases the rock beneath the surface in these zones is more decayed and less substantial than that at the surface. Exploration The first borings made with the wash rig were found extremely unreliable in the Moodna valley. That is because of the very heavy bouldery drift forming the greater part of the filling on the ancient topography. Next to the Hudson river gorge itself, no GEOLOGY OF THE NEW YORK CITY AQUEDUCT 155 place has presented greater difficulties in penetrating this drift man- tle. Boulders of such immense size occur that they have to be drilled like bed rock. In one-of the holes a boulder 30 feet through was penetrated and 100 feet more of drift found below. Progress in such ground is extremely slow and costly. This is so much the more so where as in this case there are long stretches with unusually deep cover. A glance at the accompanying profile and cross section will show a very deep and wide valley. Many of the borings are more than 300 feet in drift which almost wholly obscures the ancient topog- raphy. The present Moodna is about half as deep and occupies the extreme eastern margin of the older gorge. Tihere is a sec- ondary gorge on the west separated from the main channel by a sharp divide. A few other smaller notches in the line represent smaller tributary or independent stream courses. One of these of much interest is known as Pagenstechers gorge. The rock floor at all points except two in the central Moodna valley including its two nearest tributaries is Hudson River shales, slates and sandstones of considerable variation, sometimes much brecciated. The two exceptional borings are no. 8/A44 and no. 16/A44 on the west flank of the westerly tributary gorge, and they are in pegmatite and granitic gneiss which is in all probability the narrow southerly extension of the Snake hill ridge. Here again neither quartzite nor limestone were found on the flank, a condition that seems to support the view of a double fault along the Snake hill ridge. In striking contrast with the broad central Moodna are the two narrow and very deep notches farther to the east, the first in slates and the second (Pagenstechers) in Highlands gneiss. Special features Course of the Moodna. The chief interest centers around the Moodna channel. There are several unusual conditions, for example: The rock floor along the profile is almost flat for a distance of nearly half a mile in spite of the fact that there would seem to be every reason for a different form. The differences in hard- ness of rock floor alone would encourage differential erosion; and, since the structure of the formations, the strike, is almost parallel to the supposed course of the stream, the influence of different beds would be at a maximum. Furthermore, the deep gorge of the Hudson, into which the stream flowed is only 2 miles away; 156 NEW YORK STATE MUSEUM and if that gorge represents stream erosion to such depth (over 750 feet) it would indicate a gradient of nearly 300 feet to the mile for the last 2 miles of the Moodna—a condition to say the least decidedly unfavorable to the development of a flat-bottomed valley. Of course, if the profile as deterinined can be assumed to run exactly parallel to. the old stream channel for half a mile it would be less surprising. But even then it is too flat. For so short a dis- tance from the Hudson gorge the gradient ought to be much greater than the variation observed in the Moodna channel. There are certainly reasons in the structural geology favoring a northeast course instead of one parallel to the profile line. And if the stream really did flow across this structure, the differences of hardness of beds ought to have encouraged a much greater differ- ence in depth of channel than the profile presents. With structures all running northeast there is every reason to expect the stream to follow them. Recent exploratory data strongly supports the theory that the Hudson gorge at Storm King gap is widened and possibly some- what overdeepened by glacial ice. Under normal stream relations one might consider the Moodna a tributary hanging valley, itself rounded and smoothed to a broad U-shape by ice. This would be a very easy solution if it were not for the fact that this tributary Moodna opens into the Hudson as a reversed stream, 1. e. it opens against the flow of the Hudson and more or less directly against the known ice movement. It can not be a hanging valley there- fore of the normal sort. If a hanging valley of ice origin at all it would necessarily be one therefore gouged out by ice moving from its mouth toward its head, a case that so far as the writer knows has never been observed. The chief objection to this theory is that in no other gorge or channel (with one exception, the Hud- son at Storm King gap) anywhere in the region so far as known is there any evidence of serious modification of an original stream channel by the ice invasion. Of course, the axis of the valley is favorable and the situation is peculiar in that it parallels the High- lands front in this vicinity and the action of the ice may be as- sumed to have been somewhat concentrated along this margin hbe- cause of the obstruction. Inner notch or secondary gorge. Those who habitually em- _ phasize ice action would no doubt choose to regard this whole val- ley as shown in the profile, as chiefly glacial in character and origin. If that explanation is the true one, then it must be ad- mitted that a deeper smaller inner notch or gorge is unnecessary and indeed unlikely. GEOLOGY OF THE (NEW “YORK ‘CITY AQUEDUCT 157 The critical point therefore in the whole argument is as to the origin of the valley, 1. e. is it essentially a stream valley? Or is it as to present rock floor form wholly a glacial valley? If it is a stream valley then no doubt full account must be taken of the proximity to the Hudson, and the possibility of developing a temporary graded condition and some adequate allowance must be made for its work during the subsequent continental elevation and the deepening of that river to several hundred feet below the known bottom of the Moodna. In short, one would expect a nar- row deeper notch in the Moodna floor as a result of this rejuvena- tion. But on the contrary if in preglacial time the stream were not so powerful and had not been able to keep pace, and if the ice movement can be assumed to have concentrated along this line to such efficiency as to gouge out a groove 3000 feet wide almost flat to a depth of 300 feet only guided in direction by the original Moodna, then one may readily abandon the idea of a deeper notch. One or the other of these types of origin must be the chief factor in reaching a reasonable opinion as to the presence of an inner notch. In any attempt to choose between these factors, one is led to reconstruct the preglacial drainage lines. When this is done it at once appears as most probable that there was at that time as now a considerable area tributary to the Hudson with a stream course very much like the present Moodna. In other words a fair sized stream is assured. Once such a stream is granted and the effects of its work reckoned in full knowledge of the adjacent Hudson, and its probable behavior is studied in the light of the data ob- tained in exploration of the valleys of other tributaries, it becomes more and more difficult to wholly eliminate the inner gorge idea. It seems to the writer probable that the valley owes its erosion chiefly to the preglacial stream. But the channel has suffered sub- sequent widening and smoothing by ice especially in its upper and broader portion, below which there may yet be a notch. One must admit that the results of boring prove the notch to be very nar- wom, Ices tnan 150 feet, or else mot tere at all: In reaching an opinion as to the possibility of one so narrow, it is worth while to note that the Esopus, which is a larger stream, has cut down at Cathedral gorge to a depth of from 50 to 80 feet with almost vertical sides and only about 150 feet wide. This gorge further- more is cut in almost horizontal strata of such character that there is no special structural tendency in them to contract the stream. At the Moodna on the contrary, in addition to the smaller 158 NEW YORK STATE MUSEUM size of stream, the rocks stand on edge and run parallel to the supposed course so that this structural influence is toward a nar- row and reasonably straight gorgelike form. It is not only pos- sible that the gorge is narrow, but even probable that it is narrower than the present Moodna, i. e. less than 100 feet wide. How deep such an inner gorge may be if it does exist is a prac- tical question in this particular case, because its depth has a direct influence on choice of depth of pressure tunnel. Because of the evident narrowness it is likely that it is not of very great depth — in view of the quality of these shales perhaps not over a hun- dred feet. Is there any one point more than another favorable for such a notch? There are two facts bearing on this question, (1) the vari- ation in core saving which indicates that hole no. 5/A44 with 7% has a recovery of only 1/5 the average, and (2) the fact that hole no. 15/A44+-, which is the next hole, shows the lowest bed rock in this valley. On the ground of profile therefore and on the ground of structural weakness there is reascn to choose this space between no. 5/A44 and no. 15/A44 as the most likely position. Summary. The very abnormal profile of the Moodna valley based upon the borings may be due either (1) to parallelism with the stream course, or (2) to a graded condition of the stream in some preglacial epoch, or (3) to modification of an original less prominent channel by ice erosion. It is the opinion of the writer that the ancient stream crossed the profile line much as the present stream does, that the additional narrower valley immediately to the west side is that of a pre- giacial tributary instead of a bend of the Moodna itself, that there was a development of a moderate sized somewhat flattened valley corresponding to the benches and shelves noted in other streams, including the Hudson, that subsequent elevation of the continent rejuvenated the stream which cut a deeper narrow inner notch, that glacial ice moving in reverse direction widened and smoothed this upper portion of the valley, but that there may yet be a remnant ot the deeper notch in its bottom, and that the space between holes no. 5/A44 and no. 15/A44 is the most likely location of this inner gcrge. Tributary divide. The sharp divide between the two deep portions of the valley bottom has proven an evasive feature in the later exploration. Two holes put down a short distance to the southward (24/A44 and 20/A44) failed to find the rock floor so high, one reaching rock at a depth of 181 feet and the other failing Se ne — a te ALAN We AULA HAE es il x =%, , rn 3 A Py - 7 ; t as oa on. ~. i 4 AY ut q we 3 a ¥ eS soe WE ELE EE ~~ ae . a v a & 2 B : . r * ae ne . a Ane is i“ = SS ? Wh x ' ‘ : fs As A | . 3 i. : | Nyt a \ : — 300. 300_ SS & R “e es RS Ny Chie | i ic i ij if Wi ES i A) = Hy Wy ih iil Wl) HUN AN i 20°F (L/h ii =f il ili HN AY \\ WN Vo» NN ANN N j LY Vy Hii AN AN a eGR nae LL ANN ee) ak MMA A Hh 108 taal ANd iS oo eM Th mi Gh Uh} MN WH), Hy HY) ttt i I Hing a Ha katabelt ve Hi Hl i il HA Hh HH i) oo Ih WH My} Oe ie Mh Wl Ve MH Tin iy}! yy) \\\ Lap yO) |. J: GEOLOGI c SE CTION Oo LALMEETS jj / ili , My NANCOTT Wiha BAK icil Tg ii LLL cl QL conta OAR ak, eee y A ce Slate Slate PROFILE ALONG LINE | C-D-E-F am VERT es PROFILE ALONG LIN: nel GEOLOGY OF THE NEW YORK CITY AQUEDUCT 159 to find rock even at 213 feet. Two others nearly a thousand feet to the westward, however, found rock again at approximately the same elevation as the divide. If this is a tributary stream divide therefore it must have an east-west trend. Pagenstechers gorge This is a notch between Storm King ridge and Little Round top occupied by a very small mountain stream. The rock floor is granite gueiss of the Storm King type. Its special characters are (1) extreme shattering or crushed condition, and (2) extensive decay along this zone which has softened the rock constituents to great depth. Considering the nature of the granite gneiss in general this nar- row gorge is a surprisingly deep one. But this is no doubt due to the influence of the decayed crush zone. The drill cores taken from the holes that penetrated the floor at this place are so much altered that, after several months exposure to the air, they can be readily crushed in the hand. Hole no. 16/A45 which is centrally located penetrated to —196 feet. It is in material of this same condition, to at least —100 feet. Similar conditions are proven to the north of the line, shown in the accompanying profile and a rapid increase in depths. From the surface outcrops farther up the gulch it is easy to see that the crushed zone extends in that direction with the strongest lines about s. 70 w. This is doubtless on the strike of the fault lines of the northern border of the range. It is of more than usual interest in showing the depth to which incipient decay has penetrated in these crush zones, and the efficiency of stream erosion along them. Overthrust fault The principal fault line follows the margin of the granite gneisses. At the best exposure of it the Hudson River slates are overridden by the gneiss. This represents therefore the cutting out entirely of the Wappinger limestone and the Poughquag quartzite and a part of the slates by the displacement which must amount to at least 2000 feet and probably more. The same relation is indicated by the borings and by the outcrop near the village of Cornwall, but a little limestone is found midway between the two points along the strike of the fault. The strike of the fault averages about n. 65° to 70° e., but locally, at-the best exposure, it is only n. 35° e. The dip is southeast at an angle of approximately 45 degrees. 160 NEW YORK STATE MUSEUM Statistics Moodna valley I HOLES BORED UNDER AGREEMENT NO. 18 No Surface Rock Rock Per Ars elevation in | elevation in | penetration | cent core KIND OF ROCK feet feet in feet saved I 86 27 | 22 o | Slate and sandstone (On porosity test with plug at 58 feet deep the loss of water was 6 gallons per minute with pressure of o-10 pounds per square inch.) Test unsatis- factory because of large hole. 2 22005 i | fe) fo) | aren | 130/13 S007 26 o | Slate (On porosity test with depth to plug 173.5 feet and pressure o—60 pounds per square inch the loss was 5 gallons per minute.) Test unsatisfactory because of large hole. P4 259.6 39.4 TSA a5 ' 975 | Slate and sandstone 5 2055 B75 £2042 71 | Slate and sandstone BO2 7, P fe) fe) y| 297.0 +26 20.07 o | Slate eee eee ee 2 HOLES BORED UNDER AGREEMENT NO. 40 TFT P OOlO“ROROF#ROFNOR?eR>*OF?*ORO‘OOOOOOOooooooo oa (sao na Surface Rock | Rock. Per RAG elevation in | elevation in | penetration | cent core KIND OF ROCK feet eet in feet saved! ela 276 201 125 o | Slate pe Pipl @ 228.8 2 ay fe) a see: 204.7 257-7 45-3 Oo ae ET 4 272 at 222.1 13.0 47 60 | Slate and sandstone Ee. 5 BAG iE 220.1 48.7 o | Slate 6 374.6 250.6 38.0 fo) : | 168.4 40.4 ETOn 5 88 | Slate and sandstone Fe 8 188.7 168.2 BAS 76 | Slate and sandstone 9 One 164.3 2S o | Slate te) E7203 46.3 26 fo) a BIL 169.9 98.9 Oe we fe) os 4 12 2PM 208.2 255 o | Slate and sandstone Ate 2207, 74 TiO) 5/ 227 O io bry: 226.6 2126 pe) fe) ps Firs 230.1 215 ait 32.5 o | Slate and sandstone i {16 2O8E3 184.3 32.0 o | Slate fn 169.2 42.2 25.0 fe) ¢ 1In cases which show no recovery of core a method of drilling was employed different from the others and the rock was ground to pieces. Failure to recover core may therefore be no indication of poor rock quality. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 161 3 HOLES BORED UNDER AGREEMENT NO. 44 ———— NG Surface _ ~ Rock Rock Per . RA elevation in | elevation in | penetration | cent core KIND OF ROCK feet feet in feet saved 1y SEs ge 5O7 5 15 Slate and sandstone 12 Ee eas ETE 229.6 20 Slate and sandstone 3 282.9 205 3 58.8 14 Slate 4 277.8 S558 166.7 26 Slate and sandstone 5 209.5 ALO 50.9 7 Slate and sandstone 6 | 2790.5 — 4103 43.0 2 Slate 7 299.2 Sent 102.2 og, Slate 8 ae +89.0 109.3 57-6 | Granite gneiss and quartz 9 282.6 ge 0 go. 13 Slate and sandstone IO 230.5 —=30.5 BoA. 7 49 Slate and sandstone Pe 249.5 ens 63.5 2 Slate and sandstone 12 272.0 =k. 58.6 30 Slate and sandstone r3 288.4 She 79.0 13 Slate 14 185.1 —39.9 91.8 32 Slate and sandstone 15 301.8 —59.2 a he 45 Slate and sandstone 16 ra ae +25.9 104.6 43 Pegmatitic granite 17 300. eee 7s 2 22 Slate and sandstone ! 1 Porosity test made on hole no. rt shows a loss of .03 gallons of water under roo pounds pressure with packer at depth of 387 feet. Depth to ground water 217 feet. Porosity test on hole 2/A44. Ground water level at a depth of 90 feet = el. + 184.5’. SUMMARY Depth to packing fo) 20 40 60 80 | 100 == Gage pressure in feet 40 60 80 | Ioo | 120 | 140 == Calculated pressure! TAG) scaler re ey ee eae ae .25 -37 -50 64 79) | Geost—— callonswWost TOO. ae eee mer eee: 20 BOG] a35 42 252 .07 = ZA. «oe tep ee eh Meee oie c0eNe 09 Asie. .16 -19 323 28 < Calculated pressure equals average pressure plus weight of column of water from surface to ground water level. Gage pressure is given in pounds per square inch. Loss isin gallons per minute. 162 NEW YORK STATE MUSEUM 4 HOLES BORED UNDER AGREEMENT NO. 45 eee No Surface Nas elevation in feet Ia 426. 2 390. 3 442. 4 432. 5 433- 6 180. 7 179. 8 214. 9 179- Io 260. TE 214. 12 22 ng LO2s 14 269. I5 209. 16 28K 17 237% NHNON HDAHAPNHRH oO Cou Nn ON Rock elevation feet DO * 266. 286. 268. 207 T6n : nos” 142. alse 2eu): E55 236. 168. DNs pR TZ0 . iy Oe 387. in DN TWHWANAHO NA COMO COM Ff Rock penetration in feet humnoumonn 1 ~ Per cent core saved on p (o.0) (0) [e) (c's) (o} (0) (©) (0) (0) fo) (esy (oe) (oe) (2) (eo) (o iS O* Ke) KIND OF ROCK Slate with quartz Slate «6 Slate with quartz Slate Decayed granite gneiss Slate Decayed granite gneiss Slate “ec ec Decayed granite gneiss Decayed granite gneiss and seamy gneiss Gneiss and dyke rock CHAPTER IX ROCK CONDITION AT FOUNDRY BROOK! Foundry brook is a small stream entering the Hudson at Cold Spring in the Highlands. It drains a rather abnormally large valley’ bordering Bull mountain, and Breakneck ridge on the east, and its axis is in the strike of the principal structure of the gneisses which form the chief rock formation of the floor. This valley is in exact line with the course of the Hudson from West Point immediately southward, and its rock formations are similar in character and con- dition. There is greater variety of rock composition in this belt, 1. e. the Foundry Brook—Hudson river belt, than in any other in the High- lands of similar area. The eastern half of the belt is a typical development of banded gneisses and schists and quartzites belonging to the sedimentary representatives of the Highlands gneiss. Small layers of interbedded limestones are frequent together with serpen- tine, and mica and graphite and quartz schists. In addition along the east bank of the Hudson, they are profoundly modified by crushing and shearing in zones that trend with the formation, 1. e. in a direction leading toward and through Foundry brook valley. The west side is much less variable and is bounded at the margin by one of the most massive types of the region — the Bull mountain and Breakneck mountain gneissoid granites, which are essentially the same as that of Storm King mountain. ; But additional structures enter Foundry brook valley from the western side at an acute angle with its axis and formational trend. These additional structures are two well marked faults, which cross the Hudson — one along the precipitous southeast face of Crows Nest and the other along the southeast face of Storm King moun- tain. These are the most pronounced escarpments of the whole region. The first one crosses the Hudson between Cold Spring and Bull mountain and in passing northeastward loses much of its in- fluence upon topography and its movement is probably dissipated in that direction. A line from the southeastern face of Crows Nest to the point to be described runs n. 50° e. 1 Explorations at Foundry brook were done under the direction of Mr Wilham E. Swift, division engineer, now in charge of the Hudson River division of the Northern aqueduct. 6 163 164 NEW YORK STATE MUSEUM Explorations Foundry brook therefore contains structures that could produce considerable effect upon the quality and condition of rock floor. The rock floor is covered with heavy bouldery drift—thicker on the Bull mountain flank than in the valley bottom proper. Where the aqueduct line ‘crosses the floor is at an elevation of 200 feet to 350 feet A. T. Hydraulic grade of the aqueduct is about 400 feet. The lowest bed rock found along the line is 182.2 feet and the channel of the present stream coincides with the preglacial one in that portion of its course. There are two secondary channels — probably tributary stream channels on the west side. One of these lies under 70-80 feet of drift. Borings were made for the purpose of determining the rock floor profile and the condition of bed rock. In most of them the ordinary gneisses and granites were penetrated in normal condition. But in a few a very unusual condition was found. Hole no. 2 at el. 347 feet near the west or Bull mountain margin penetrated 49 feet of drift to el. 298. Then the drill passed into gneiss which was at the top, the first 30 feet, of a fair quality. This is shown by the core recovered —the first 12 feet recovering over 50%. But the percentage of recovery rapidly fell off — amounting to only 36¢ in the first 50 feet. Only 1 foot of core was recovered in the next 30 feet, or only 3%. While from that point el. 220 feet to the bottom of the hole el. 51.8, at a depth of 295.7 feet from the surface, nothing but fine decomposed matter was washed up. There was no core at all. This was at first reported as sand by the drillmen, and, coming at a time when exploration of deep buried gorges was the rule at other points of the aqueduct, there were many questions about the interpretation of this new hole, the first assumption of the drillers being that an overhanging ledge of a very deep gorge had been penetrated passing through it into river sands below. A little study of the material proved that this view is untenable. The sandy wash from the drill is true disintegrated gneiss much decayed and dislodged by the drill. But the meaning of it and the extent of it are after all important additional questions. Interpretation and further explorations It is certain that the soft material and the “‘ sand ” reported from this boring represent rock decay induced by underground water circulation. Water circulation is rather free as is shown by the 165 GEOLOGY OF THE NEW YORK CITY AQUEDUCT ‘sSuliog Aq poyeoipul se Adyyea Yoo1q Arpunoyy fo j[rejop [eanjonsaysg 6z “sty 7ane7 was MOON AYGNNO J J SONIYOE ONY 3140Ud pooy ! pasovusorag | BH 707 us yoy si da SS/BUD PrysoM|. Wey p4so7/ : ' 9056/7 (7 7 70 8 OIA LY OH“) : = cy) ie f y zy4000 * || shor of Bal Lia Sesausy worgspued SRO | | J®9S.bL PBL PACPIN PLOT ¥h30%9 PIT9A05 oF Mossy sus0es Vado a Fusmo peusergo a9 f/702 249 Show eu gyhspaayred YLIM os ysdod 4a%p/ (PFOL So4fU/ a+ S rv ow rere priee 4 ig (JAB 4A ==> . le ee NwismLxy - oa: 682477 OS 4EPK1F ES 166 NEW YORK STATE MUSEUM fact that there was an artesian flow from this hole of 10 gallons per minute after reaching a depth of 80 feet, which increased to 1 5 gallons per minute after reaching a depth of 253 feet. This under- ground supply is maintained since completion and the pressure is sufficient to raise the water about 15 feet above the surface. This is a behavior that is consistent with the geologic conditions. The boring has no doubt penetrated a crush zone following one of the faults which enters this side of the valley. The crush zone dips steeply and the boring has penetrated the hanging wall of more solid rock in the first 50 feet and, after reaching the broken and decayed portion of the zone, has swung off parallel to the dip and avoiding the more resistant foot wall has followed down on the soft itiner streak. 2 y uv a 9% o£ Ns peel GS Le a Ss oe L ye Se ae ie x x : ‘ granite \ Deflection of drif] xin clecayed Zones Pe Tock: villey indicate vie rela tipeter Geertatn weenie oy thenena aise supposed ~ influence in deflecting the drills A i This crush zone extends on northeastward across higher ground where opportunity for taking in surface water is offered. This is without doubt the source of supply for the circulation which fur- nishes the artesian flow and which has been so effective in pro- ducing decay to great depth. But the circulation and associated decay are probably limited to comparatively narrow zones. There is no good reason for assuming large masses of rotten gneiss at great depth. The worst zones are narrow but may be comparatively deep, i. e. they may extend much deeper than any of the borings yet made in this valley. The depth of decay is related to the outlet for underground circulation which in this case is the gorge of the Hudson. GEOLOGY:OF THE NEW YORK CITY AQUEDUCT 167 Several other borings encountered similar conditions, especially those on the west flank of the valley within range of the belt in which the fault seems to be located. Hole no. 9 reached the rock floor at a depth of 80 feet, and then penetrated rock to a depth of 159.7 feet. All of the material is badly decayed. Only 1 foot of core was recovered from the whole boring and that is mostly quartz coming from a veinlet or peg- matitic streak at 141 feet. Water under slight pressure was en- countered in this hole also. But because of the somewhat greater elevation Gt tie surface at this than at hele no. 2 there is not a constant outflow. Two other holes immediately to the west show much better rock condition — no. 1 showing 79% core recovery. Also two on the east side at greater distance [see accompanying profile] show good rock. But one other no. 3 at a distance of over a thousand feet to the east encountered another zone of decayed rock, the record being very similar to no. 2 in that poorer conditions are shown at depth than near the surface. Rock was found at a depth of 20.2 feet. .From 20.2 to 116 feet the gneiss was quite hard, 55.3 feet of core being recovered or 57.7¢. But from 116 feet to the bottom 207.5 feet the material was as bad as in hole no. 2, and no core was recovered. Several other tests were made on the borings with a view to de- termining the character and extent of these features more definitely. For example, if the interpretation given for the behavior of no. 2 and no. 3 is correct it ought to be possible to survey the holes and determine a deflection from the vertical as the drill deviated from its course to follow the softest streak. A survey conducted for this purpose indicates just such a result. The accompanying sketch shows the data plotted. The drill was deflected 4° 36’ at a depth of 50 feet, 7° 36’ at 100 feet, 8° 2’ at 150 feet and 9° 40’ at 198 feet. Pressure tests were made for porosity. on some of the holes in sound rock. Some of these data are given on the profile. Some of the rock of this valley, if very extensive, such as that in borings no. 2, no. 3 and no. 9, would be very poor ground for tunneling. The practical question involves especially the width of these zones, are they a foot wide or are they a hundred? In an _ attempt to help settle that question an inclined hole was proposed that was to run at an angle low enough to crosscut these belts. Accordingly hole no. 14 was bored inclined 40° 26’ to the hori- zontal and started on the solid granite gneiss. The results were not Se Re ge bees emt bee TTS ES SSE eet 168 NEW YORK STATE MUSEUM ‘ Jnelin. 7 “36, S.30°9'W, “a ~ $ = | 8 = | x iO a | ~ [rae 822" Jaclin. 2-36 S/6-37W. S 35°45 WS 5 Ioclin. 7°85 S76 230'wJf~ SKETCH SHOWING DE- FLECTION OF HOLE 110.353 AS DETERMIN- EO BY CLINOMETER. Inclin, 9°40" Scale: |= jo’ S.23°26' lo han Ne Figure 31 GEOLOGY OF THE NEW YORK CITY AQUEDUCT 169 very encouraging. The decay is shown not to be confined to mere seams. The doubt raised by so much bad ground has finally led to the adoption of a different plan for crossing Foundry brook valley and no further data are likely to be added by this work. As it now stands the borings at Foundry brook indicate the deepest decay of any yet made in granites or gneisses except those of Pagenstechers gorge on the north side of Storm King mountain. Both cases are of similar origin and history, but Foundry brook is apparently the more complex in occurrence. There are several parallel zones along which there is extensive decay to a depth of more than 300 1 hese eS af rey 53) Lose aD. are 4, Aaa pec Fa ret, i a Tee ~; At f . ; we bt eae he ; a shia an i : VS eels de ote 2 corr = aoe ‘i tty a7 ¥ > oa : i. ae : rey! ° CHAPTER X GEOLOGY OF SPROUT BROOK Three creeks unite to form an inlet at the sharp bend in the Hudson immediately above Peekskill. The middle one of these is known as Sprout brook. It occupies a deep and narrow valley that is well marked for 10 miles in its lower course and is trace- able as a physiographic feature of less prominence to the north mar- gin of the Highlands. Its persistence indicates some important structural control in erosion. . Geology This valley lies in the midst of the most typical gneisses and granites of the Highlands region. And in addition several of the “iron mines” of Putnam county lie on its western flank. The rocks are complex granitic and quartzose gneisses and granites. Foliation and banding and bedding wherever this appears is parallel to the axis of the valley. The most notable geologic feature is the occurrence of a broad belt of crystalline limestone throughout the lower 4 miles. It is undoubtedly chiefly this limestone, which is less resistant to weather than the gneisses, that controls the form and size of the valley. As to geologic relations, this is one of the most interesting formations of the region. It is coarsely crystalline, full of silicious impurities at many places and carries small igneous in- jections and dykes, and so far as the bedding can be followed, stands almost on edge. Although an actual contact is not seen, at several places the limestone and gneiss approach within a few feet of each other and it is certain that no other formation can come between them. This is more certainly indicated in the northerly extension of the valley where the limestone gradually disappears leaving only the gneisses and granites. That there may be a fault contact must be admitted, but of this there is no good evidence in the field. Such relations and character show that this limestone is similar to the smaller interbedded occurrences noted frequently with the gneisses in the Highlands and elsewhere. [Ii it is of that type then it is the largest representative yet found in that series. But it is also in these characters similar to the Inwood limestone of more southerly areas. The overlying Manhattan schist which is lacking 171 172 NEW YORK STATE MUSEUM may have been removed in erosion. One of these types it resembles, but it can not be the Wappinger (Cambro-Ordovicic) as was pointed out by the writer in a former report.1 The Wappinger, wherever known to be such, is never intruded and always lies above a thick quartzite (Poughquag). It does so even in the next valley (Peekskill creek) less than a mile distant. With the interpretation of this Sprout Brook limestone therefore is involved the correlation ard interpretation of the age of much greater areas. That the Sprout Brook limestone is not Wappinger is clear enough, but it cculd be either interbedded (Grenville) or Inwood. If it is Gren- ville then of course it has no direct bearing on the Wappinger- Inwood question and these two might be equivalents. But if the Sprout Brook limestone is not Grenville (interbedded) then it must be Inwood and in that case the Inwood and Wappinger are not equivalent — which means that there are two series above the gneisses instead of one—an Inwood-Manhattan series, and a Poughquag-Wappinger-Hudson River series. At the present time it is not possible to give with certainty a final interpretation of the Sprout Brook limestone. Explorations * It was at first believed that a pressure tunnel could be con- structed advantageously at the point of crossing this valley and borings were made to test rock conditions. The data gathered in exploration are indicated on the accompanying geologic cross sec- tion jfig. 32]. Borings indicate that the rock floor has been eroded to a few feet below present sea level and that the gorge has a drift filling of more than 150 feet. The central borings penetrate limestone and indicate a total width of this type of more than 400 and less than 600 feet. The best estimate on the basis of these explora- tions is 500 feet. Whether this width represents one thickness of the formation as would probably be the case if it is an inter- bedded Grenville layer, or part of a double thickness due to infold- ing, as would probably be the case if it is the Inwood, there as no evidence. The thickness seems to be even greater farther south in the same valley (it becomes ™% mile wide), but it can not be eg 1 Structural and Stratigraphic Features of the Basal Gneisses of the Highlands. N. Y. State Mus. Bul. 107 (1907). p. 361-78. 2 Explorations at Sprout brook are in charge of Mr. A. A. Sproul, division engineer in charge of the Peekskill division. 173 GEOLOGY OF THE NEW YORK CITY AQUEDUCT jonponbe [Psy oy JO ssutsoq A1Oje10[dx9 9y} Aq pozvorpur sv Yoosq ynoadg fo uoTdas sso1d d1B0Joon Zé HN THOAG AWS — i eh ram Ws Li ik if ( iN i ae -—————— | Oe" teed hava weet 1] QO ay et 4 r] ! ‘4 Meemaet Ph mi moet es) soa moni! ie % PA = A 44459 ILe chek? ty v) 79 Mo%eol mii 22/I me aula 2% a9 be tae Teva pe ‘ \ ORTTTE er a al iH OL7, 1007 PPL 2/ SL 100 OF 1BPOI1T Ty tet07 of” - p BPE IT BF gm 1 9PFO/7F Pin 1 PFE TITFI, » FOR /F Py ZEAL FOZ ~7bLtTF rae 12 S“77F By OSL TF iP IEAIa &¢ CBW7 Besa PAO PEY AY — 1Oof7 — | reeaKer Zs vn 171 2h 174 NEW YORK STATE MUSEUM accurately measured and there is no way of guarding against repe- tition of folds. The valley floor is decidedly terraced at an ele- vation of about 130 A.T. One side is limestone and the other is granitic rock. This is probably a local mark of the Tertiary base leveling work. Because of the great depth of this narrow gorge, it would require a 500 foot shaft at each side to lead from hydraulic grade down to a safe level for the pressure tunnel. For a crossing not more than 2000 feet long this is excessive and the cost becomes greater than by other methods of construction. Consequently the tunnel plan has been abandoned and it is not likely that further data bearing upon these questions will be added. CHAPTER XI STRUCTURE OF PEEKSKILL CREEK VALLEY Immediately east of Sprout brook, described in the previous sec- tion, is Peekskill creek, which drains the largest valley emerging from the southern margin of the Highlands. This valley as a physiographic feature is continuous with the Hudson river gorge from the sharp bend at Peekskill to Tompkins Cove. There are important structural features along the strike of this valley which extend very far beyond the limits of Peekskill creek itself, among which are strong folding and block faulting. The chief fault con- tinues to the southwest with still greater prominence and appears on the west side of the Hudson in the escarpment forming the southeastern margin of the Highlands continuously for many miles into New Jersey. Near the Hudson, Peekskill creek and Sprout brook unite and the structures and formations characteristic of each valley converge until in the last half mile of their united course rock formations characteristic of Sprout brook lie on one side of the valley, those characteristic of Peekskill creek on the other, and the contact which follows the divide to that point then passes beneath the waters of Peekskill inlet. Because of the block faulting which has carried down overlying formations and protected them from the total de- struction characteristic of the central Highlands region this valley is of unusual interest. Explorations * The aqueduct line crosses this valley about 3 miles from the Hudson, and in determining the possibility of crossing by pressure tunnel in rock a considerable number of explorations were made. Enough has been done to outline the rock floor profile very defi- nitely and to determine the condition of the formations. An examination of the drill cores and records of eeratians shows the following facts which are compiled as fully as possible on the accompanying cross section. Phyllite. One boring (no. I) is in a phyllite whose character and relation to other formations leads to the conclusion that it 1These explorations were directed by Mr A. A. Sproul, division engineer of the Peekskill division with headquarters at Peekskill, N. Y. 175 176 NEW YORK STATE MUSEUM belongs to the Hudson River slate series. This type of rock forms the whole western side of the valley for several miles. Beds stand on edge or dip steeply southeastward and are in good sound physi- cal condition. The rock is everywhere a fine grained micaceous slate or phyllite and in some places carries pyrite crystals. It is impossible to estimate the thickness or minor structural habits. But it is clear that it forms the upper member of a series that has a synclinal structure and therefore the belt represented by the phyllite marks the axis of the syncline although the chief val- ley development lies wholly to one side. Limestone. Eleven borings (no. 2, 3D, 4C, 11, 13C, 18, 22, 23, 25, 26 and 29) are in limestone. All show essentially a very fine grained close textured crystalline gray or white or bluish rock with strong bedding standing nearly vertical or at very high angles. This, because of its character and relation to other forma- tions, is regarded as the Wappinger limestone —a formation well known north of the Highlands, where it is at least 1000 feet thick. From present explorations it is now certain that a belt 3250 feet wide is underlain continuously by this formation standing nearly or edge. Unless repeated of course this would represent approxi- mately the thickness for Peekskill valley. But it is not believed to be so thick. It is more likely that there is a threefold occur- rence brought about by close isoclinal folding (a closed s-fold) as seen in the accompanying cross section. This view is supported by at least one occurrence of the underlying quartzite member near the center of the valley at a point a couple oi miles farther north On the line of exploration, however, none of the borings pene- trate any other formation beneath. Attention is called to additional structural details and physical conditions in a later paragraph. Quartzite. One boring (no. 5) is in a quartzite. It is very pure, fine grained, closely bound and typical quartzite. The beds stand almost vertical and the whole thickness is known from nearby outcrops to be approximately 600 feet. From its character and re- lations to other formations it is regarded as the Poughquag —a well known formation of the north side of the Highlands. Gneisses. Five borings (no. 7E, 9 B, 17, 27 and 28) are in gneisses. These are to a considerable extent simple granite gneisses of igneous origin. But there is the usual variety characteristic of the Highlands gneisses and no doubt they are representatives of the great basal gneiss series that is elsewhere referred to as the equivalent of the Fordham of New York city. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 177 2 Stratigraphy This is therefore the rock series of Peekskill creek. It is the only locality on the south side of the Highlands where all are represented in complete and simple form. ‘There is no doubt that it is the Poughquag-Wappinger-Hudson River series, in spite of the complete absence of organic evidence. A similar though not so complete and clear occurrence is to be found on the west side of the Hudson near Stony Point and Tompkins Cove. That is a part of the same structural syncline. It is probable also that the phyllite so finely developed in the village of Peekskill in the next small valley to the east is the same. But outside of these occurrences there are none that clearly represent this same series as a whole and in the same condition. No more striking example of this fact can be found than the adjacent Sprout brook described in an earlier section. There coarse crystalline and injected and impure limestone occurs alone — no phyllite and no quartzite. When one remembers that the two occurrences so strongly contrasted, Sprout brook and Peekskill creek, converge until they actually unite, and still preserve their stratigraphic dissimilarity, without any adequate structural reason for it, the only conclusion possible is that the two occurrences rep- resent two entirely different series of formations. The Peekskill valley series 1s Cambro—Ordovicic in age; what is the other? It is older, at least that is certain. But is it (the Sprout Brook limestone) as old as the oldest of the gneisses themselves and therefore interbedded with them representing locally the Gren- ville; or is it intermediate — Postgrenville and Precambric — with which possibly other occurrences of rocks of similar habit and equally uncertain relations belong? It is on the general similarity of this occurrence to the Inwood limestone as known throughout Westchester county and New York city that a tentative intermediate series has been recognized. This is the Inwood-Manhattan series. Whether it is in reality a separate older series is not regarded as proven. But for engineering and practical purposes the distinction is a good one and eminently ser- viceable. Further discussion may better be continued in a different publication. 3 Rock surface The bed rock surface is pretty well outlined by the borings. A profile based upon them seems to leave no unexplored space of suf- ficient extent to admit a gorge of great consequence to a lower level 178 - NEW YORK STATE MUSEUM than is already shown in holes no. 1 and no. 11 [see profile and cross section, fig. 33]. The elevation indicated by no. 3 D is be- lieved to be misleading because of the use of a drill that was capable of destroying a part of the ledge rock that would usually core. The points believed to be weakened by structural disturbance and therefore most likely to be attended by erosion and stream action are in the vicinity of hole no. 11, near the present creek, and hole no. 25, near Peekskill Hollow road. 4 Buried channels | From the accompanying cross section it will be seen that the drift cover is more than 100 feet thick over large portions of Peeks- kill valley. The rock floor in the middle of the valley averages approximately 25 feet A.T., while the drift surface except where cut out by stream erosion is at about 125 feet. In the rock floor there are two depressions, the large one wholly within the lime- stone belt and the smaller following the limestone-phyllite contact. There is not much difference in their depth so far as explored, but there is a possibility of a somewhat deeper notch in each one. The depth to which some of the limestone beds are decayed by under- ground circulation would lead to the belief that a deeper notch may exist. The drift cover is chiefly partially assorted sands and gravels in the central portion of the valley, and more of a till on the eastern valley side. It is noteworthy that the present Peekskill creek lies far to one side following closely the phyllite wall. : 5 Underground water Present elevation above sea level is so slight that there is appar- ently little encouragement of deep underground circulation. But at certain points the rock has been found to be very badly decayed ‘to a great depth—to at least 200 feet below sea level. This is ‘believed to have been accomplished chiefly at a time when the re- ~ gion stood at a higher level. Hole no. 22 is especially notable in this connection. A comparison of the figures of core saving is one “of the best lines of evidence on this question. Wherever data are at hand the percentages of saving have been put on the cross sec- tion. Hole no. 29, for example, shows a saving of only 11% in the \lower 250 feet, reaching a depth of 207 feet below sea level. The-present water table profile is shown on the cross section. A ‘great body. of water stands in the assorted sands directly upon bed GEOLOGY OF THE NEW YORK CITY AQUEDUCT 179 rock forming essentially a great reservoir of supply that has ready access to the almost vertical limestone beds. This will give a maxi- mum water supply to holes that penetrate porous or broken por- tions of bed rock. The attitude of all strata is especially favorable for admitting an almost inexhaustible supply from a considerable drift-covered area within which circulation is probably very rapid. 6 Condition of rock All strata of this valley stand so nearly on edge that drills actually explore a very limited portion of the whole series of beds. No very great advantage is gained by excessively deep boring because the drill follows necessarily almost the same bed from top to bottom. At best only the immediately adjacent beds are penetrated. This means that much of the total thickness of beds is untouched by present explorations, and must be interpreted on the basis of their general likeness to those more fully determined. The usual suc- cession of beds is known to be quite uniform in quality and loca- tions where they can be studied and there is no reason to expect greater variation here. Deviations from such normal or uniform conditions are mostly due (a) to local development of mica from recrystallization of 1m- purities in the limestone, and (v) to crush zones developed in the process of folding and faulting which has broken the rock or weak- ened it enough to permit a more ready circulation of underground water. Wherever either of these structural conditions prevail, the rock has been excessively decayed, or disintegrated, or sufficiently weakened in its binding matter or its sutures to crumble in the hand ‘or break down to a sand under ordinary boring manipulation. This’ condition; is known to reach to —297 feet. How much deeper is not known. ' Probably the decay dates back in large part to pre- glacial continental elevation at which time probably there was more ready. deep circulation with possible outlet in the Hudson gorge. This action has been all the more effective by reason of the attitude of the beds. They stand so nearly on edge that they present all their weaknesses of bedding and sedimentation structures to the destructive surface agents. They admit surface water readily and favor abundant underground circulation. Corisiderable faulting occurs. The contact between the eranite- gneiss and quartzite is a fault contact. Wherever seen this is sound. But.a crush zone in limestone lies nearly central in the valley, cut by holes no. 23 and no. 25, where the rock shows a finely brecciated WNPONbY [LAS OY) JO OUI] Ol) Suopw Ao[[VA [[PASYxoo] SSOsov sHutsoq Jo [IVjop puv UOTjo99s ssod9 o1Boloor, LE ‘Br, MUSEUM YORK STATE NEW au) (Ney NN yen Op AN Sy fet ed Mt Nae ant i} \ \ \ \ La ae a \ 4 . he omy Roy \ My 2h. Ave OPES MOTION FUSE I FS 9 ‘ eau ay Wi nee 12 1 Md, ha al (omg Gi S| oer 7 07 nen Uae int \ MIZAD TTY SH F- \\ — & GEOLOGY OF THE NEW YORK CITY AQUEDUCT 1&1 condition some portions of the drill cores being literally crushed to bits. In one hole, no, 11, near the. phyilite-limestone contact, a soft, sandy condition was encountered at a depth of 133 feet, permitting the drill rods to be pushed down without boring at all, 60 feet ahead of the casing. This, however, is not believed to indicate any very extensive weakness. It is probably connected with the bedding planes or joints rather than with general decay or faulting. Four or five inches of solution and disintegration along bedding planes would account for all that has been proven. The fact that the rods could be shoved down 60 feet while the corresponding outer casing could be shoved down only half as far seems to support this view. Summary If a tunnel were made across this valley there would be approxi- mately 1100 feet of it in Hudson River slate (phyllite), 3250 feet tn Wappinger limestone. 600 feet in Poughquag quartzite, and the rest in the gneisses. Some weak rock-is certain to be found, especially in the vicinity of station 367+50 and 345+00 to 350-00. At both places increased water inflow would be encountered with almost exhaustless supply from the sands that lie on the rock floor above. At about this stage in the exploration the Board of Water Supply decided to abandon the rock tunnel plan. The conditions found were considered by them too questionable. Steel pipe construction is to be substituted. As a result it is not likely that much more detail will be added to the structure of this very complex valley. Nom axd | rine : gel ar a ade ¥ i? és Ny : ve nm] Mtge ‘ ie #4 7 = y CHAPTER X11 CROTON LAKE CROSSING It is proposed to finish Ashokan reservoir and the Northern aque- duct first. This so called Northern aqueduct reaches from the Cats- kills to Croton lake. Croton lake is the present supply of New York city and is already connected by two aqueducts with the city distribution. As a first step, therefore, and as an emergency meas- ure the Catskill water will be delivered to the Croton system by finishing the Northern aqueduct first. As rapidly, however, as the whole project can be carried out the so called Southern aqueduct will be constructed to continue the Catskill water independently of . the Croton supply to the city. The Southern aqueduct department has charge of the line from Hunters brook on the north side of Croton lake to Hill View reser- voir near the New York city boundary. During exploratory work it has been under the direction of Major Merritt H. Smith, depart- ment engineer, with headquarters at White Plains. Construction now going on is in charge of Mr F. E. Winsor, department engineer. The first link in this southerly extension is to be a tunnel be- neath Croton lake through which the Catskill water may pass in the same manner as it crosses other valleys. This crossing has been located a short distance below the old dam on the Croton, about 5 miles up stream from the Hudson. The problems involved at this point include (1) a determination of the kinds and quality of rock to be penetrated, (2) their water- carrying capacity, and (3) opinion as to the proper depth for a successful tunnel. Geological features The Croton valley is one of the very few in southeastern New York that actually crosses the geological formations and major structural features instead of following parallel to them. In its lower portion it passes from gneiss to limestone and to schist sev- eral times. The reason for this somewhat abnormal course is preb- ably the development of weak zones by fault movements in this transverse direction. Only one of the well known formations of rock is exposed in the immediate vicinity of the tunnel site. This is the Manhattan schist, the uppermost formation of the region south of the High- lands. Along the Croton it varies greatly, the chief type being a 183 NEW YORK STATE MUSEUM 184 Ajddns |[rysywy oy} JO sjivd pojviosse puv jonponbe usoyynog oy} Jo dew uoyvooyl [esousr bel ‘Ory SNe ' 3 i) C061 '| AUVANYE OL ey) woshg NOILV9O1 YOd GIATAUNS S3NI1 LONGANOV TIDISLVO ul Ui! WD VaOvdd VD r ty O- LV NOLOUD Oy. seywn SLO NMOLNUO ye 7 —\, SS Isuvos O Sas ‘i NONUSA ‘LW s , O- J Sa eS See 9 § NMOLAYUVL S\ ey | 2 AUUG SHA A UTOAUISIH Ss VW “~~ Lo SiitisiN ati NOLOUWD s MOOR WF o. ov uoydig J me ( [PUUN] APAUH es: JIAO PUR ND GEOLOGY OF THE NEW YORK CITY AQUEDUCT 185 garnet-bearing quartz-mica schist varying from rather fine grain and semigranular appearance to a very coarse and strongly foliated structure. This part of the formation undoubtedly represents re- crystallized or metamorphosed sediments. But associated with this facies there is a more dense black hornblende schist that, not only here but at many other places, is thought to represent igneous in- trusions that have been metamorphosed together with sediments of various types, until both have lost almost all of their original char- acters. The hornblendic schist type is not so extensive as the other, the mica schist, but it is more compact and here as usual is in the better condition. Pegmatite stringers occur abundantly, especially in the mica schist varieties. They are of no great consequence, however, as a factor in this study. They originated in the aqueo-igneous activity in- volved in the recrystallization of the rock when it was worked over into a schist. Beneath this Manhattan schist formation lies the Inwood lime- stone, a bed probably at least 7oc feet thick. But at this point how deep it lies and at what depth it would be penetrated nobody can tell. None of the drills have touched it. Beneath the limestone in turn lies the granitic and banded gneisses belonging to the Fordham gneiss serics, the lowest and oldest of the region. Along the Croton river nothing but Manhattan schist is to be seen at the surface for more than a mile above and below the proposed crossing. The same thing is true for an equal distance on opposite sides from the river at this locality. But the structure is folded and the normal northeast-southwest trend of the folds crosses the river, every arch or anticline tending to bring the limestone and gneiss nearer to the surface. One of these folds does expose the limestone and gneiss in a strip extend- ing from the Hudson river northeastward for two thirds of the distance to the old Croton dam. But before reaching the Croton valley this fold pitches down toward the northeast beneath the Man- hattan schist and passes under the present lake (or reservoir) in that relation, not reaching the surface again for a distance of about 6 miles. At least one more fold is known to behave in a similar manner as it reaches the Croton. These facts make it certain that there is limestone beneath the schist in the vicinity of the crossing, and that it comes nearer to the surface in that vicinity than at some other places. South of the Croton there are several small cross faults run- 186 NEW YORK STATE MUSEUM ning nearly east and-west. It is believed that similar movements have affected the rock in the Croton valley itself, modifying its con- dition so much as to control the course of the stream. The only immediate bearing upon the problem of the Croton crossing is the question that it raises about the quality of rock and the necessity that is introduced of trying to determine whether or not there is shattering enough to be very objectionable. Explorations and data Six drill holes have been made on this proposed Croton lake crossing — one on either side just at the margin and four others within the intermediate space of 1400 feet. These inner four have been made from rafts floated on the lake and have penetrated water, drift cover, and rock [see accompanying profile and cross section, pe 27}: Rock floor. The depth of the preglacial Croton valley is pretty accurately determined at o feet or sea level. There is no reason to expect a gorge or inner channel of any consequence. The drills have penetrated only one formation, i. e. Manhattan schist. These test holes are believed to be near enough together to eliminate the possibility of any other formation appearing at tunnel grade. Rock condition. The two varieties of schist (1) the coarse garnetiferous quartz-mica rock, which is a metamorphosed former sediment, and (2) the darker, close grained hornblendic rock that is believed to represent an igneous intrusion, both occur in the cores brought up by the drill. Either under normal conditions is a good rock. But there are considerable differences in the physical condition of the rock. Holes no. 3 and no. 4 at the two extremes, on the lake borders, show sound rock that comes up in large cores with very high percentage recovery. This is confidently believed to represent the average condition of the rock in this vicinity at the sides of the valley. The central ‘holes, however, nos. 1, 2, 5 and 15, all show more broken ground. Of these holes no. 2 is much the most broken, the core recovery being only 14.8¢. The pieces are small and many are smoothed (slickensided) by movement. ‘The hole penetrates a typical crush zone resulting from slight faulting movements, and the low saving is due to the fact that the incipient fractures are not well bound together. (rehealed) by later mineral change. They are probably connected with the latest movements of this kind. ‘UOTJIPUOD YIOI o[qvjzins toy yJdop pur ‘uorZVLpNd.A109 JOyVM oqvqoid ‘yor poysnso fo juo}xX9 puv uor}Isod ‘19ACd 4yIIp Jo yydop AYoITyD SI9AOD ApHys oY] ‘SoljaMvVaA opuosjq “UTOY PUL VoTUt YO FO 4SIYOsS ULjJeYURIY [[V St IOI YT, “UIVse opLIS O} OSII ][IM JE O1OYM OpIs YNOS 94} 0} oanssoid Fopun JoyVM [Lys oy} Ativs puv ‘y1oX MoN Jo ATddns 10}vM JUoso1d oy} ‘oyv] U0JOID Yyyeouoq ssvd Oj St jouun} oT LONGINOW IIASLV) AHL &O ONISSOUD AHL LV AYTIVA NOLOXD AHL 40 NOLLOIAS ssou’) Wwo/g01080 Ow/st0WD nr? wos0U? LINGINOV TIASLVI A14d08 WILY 40 Onrod raga) 906 16 Adenupp jo say499 4 f0 {40do4 puosas Auwduo22» ay acon SOUOZ YSN LIMOU)Y] = 2. $0U02 YSNID /OUOISDIIO JO SIM] eGOGO41 — ———— ——— PLL Z/9/- ae [BUN 40f 014220) {Saq 40 ol/aZ 009 ,99)| ; ‘9109 er) PasaAoras , Pas9A0204 / ; : 3102 4 ONE 9102 %02 Up OluJoy 451IG Lib ouLiby ayf of Puibuojag 4826 2puaqusoy pup {syd Dap -24PN SnosayYeusoo _....2pR/b__ g1004P4H.. Mint Hype MI A 3 LZ ajelg ) My “7 Pat =) 4 “uv @ % Taw =j ’ 5 GEOLOGY OF THE NEW YORK CITY AQUEDUCT 187 _..The commonest secondary mineral now filling these crevices is chlorite, and, although it may completely fill the crevices it has little binding strength. Any new disturbance or strain readily causes separation along the same original lines. But in spite of the fact that the core is broken into small pieces and shows so low percent- age of recovery it is quite certain that the rock itself is not badly decayed. An examination of one of the most doubtful looking cores from the lower part of hole no. 1 showed under the. micro- scope little evidence of serious decay. ‘This is believed to mean that underground water circulation is not as abundant as the fractured condition of the rock would lead one to expect. Further- more, an examination of the cores in greater detail shows beyond question that much of the fracturing is entirely fresh and must have been done by the drill itself. It is certain that the low per- centage of recovery is in part due to this cause. The small diam- eter of the intermediate holes is contributory to the same results. Some allowance must also be made for the difficulty of working a machine from a raft on the lake. Comparison of the cores shows a decidedly higher percentage of core recovery, and presumably therefore of rock solidity in all of the other three holes — no. 1, no. 5 and no. 15. Hole no. 2—core recovered 14.8% “no. I— _ 34.6% “no. 15 — i 26.3% “no. 5— = 38.9% It therefore appears that the last three penetrate rock that is more than twice as good in its capacity to stand drilling disturbance. A comparison of quality at different depths is believed to be still more encouraging. The upper portions of all holes have poor recovery and comparatively poor looking rock. But in depth there is a marked improvement. In view of the fact that the tunnel will undoubtedly be located somewhere below the —75-foot level, it is really only this lower sec- tion that is of vital importance to the project. A tabulation and comparison of core recovery from these lower portions is given below. I From total depth of hole 2 From depth —75’ to bottom Hole no. 2— = 14.8% core recovery 25% core recovery “ 10. I— == 34.6% ~ 45% , Hoehne) TS." == 36,39 . 66% * ify no. 5 enw — 38.9% se 42% &é iss NEW YORK STATE MUSEUM Under the conditions of work, this is a fair saving and indicates much more substantial rock below the —75’ level. There are many pieces 10-12 inches in length and ior a 1 imch core this may be considered very good. It is clear, however, from a detailed inspection of the cores, that there is considerable variation somewhat independent oi depth. There are occasional stretches of poorer ground in the midst of comparatively sound rock. This is believed to imdicate that the crushed condition is confined chiefly to certain zones, and that these zones dip across the formation and across the holes at an angle. They are probably distributed promiscucusly throughout the central portion of the valley, but are certainly more abundant and more strongly marked im the vicinity oi hole no. 2 than at any other poimt tested. The rock profile shows that hole no. 2 has also the lowest bed rock. This is a further support to the general explanation of the valley as given above. The chief elements of uncertainty remaining after the borings have been completed are: 1 The exact extent or widths of the chiei crush zones 2 Their dip and strike 2. The possibility of others not yet touched 4 The permeability of the rock for underground water 5 The supporting strength oi such rock m a tunnel of large dimensions In spite of the uncertainties enumerated, the conditions are ertirely understandable. There is little probability of findmg a worse condition than that shown in hole no. 2. The permeability or porosity of these zones is of course unknown. The chief reason for believing that underground circulation is not abnormally heavy ts the observation that the joints are well filled with chlorite and that other decay 1s not at all promiment at the lower levels. Further- more, the rock is a crystalline type of rather successful resistance to ordinary solution agencies and therefore may be depended upon to hold its own im its present condition indefinitely. But because ei the poor binding effect of the chlorite it is to be expected that blocks will fall irom the rooi of any tunnel where it passes through a crush zone. Timbering will be required for protection in places, but the ground will not cave or run. These zones may be expected throughout a total distance of about 7oo feet—1. e. the space between no. I and no. 15. The chief belt of such ground probably lies between holes no. 2 and no. 5. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 189 Summary The lowest bed rock is about sea level. This pressure tunnel will cut only Manhattan schist. All rock is good ground for such work, except in certain narrow zones where it is crushed. The extent of such broken ground is not closely delimited, but occurs at intervals for a distance of 700 feet. The amount of underground circulation is judged to be moderate at —100 feet. The tunnel should be located deep enough to take advantage of the improved rock conditions shown at about —1o0o feet. There seems to be no marked improvement below —100 feet as deep as the drills have gone. ” LP Ai fi ‘ o au ye H A, tery, we! co iu iW ne : say = oa ae Wh OV Gls ach, As ites ar AM a es i, > ‘ eons a Jee Lae eae ane ah) SU Map hee : hh) : . [ i y vo i ore Ae Beg ts + Ol beu cape) ee, hl Pa Yahya tf . Maks CaN ae ps aR eae ‘ai : wD ; ve 4 nt oe , \ / 7 aden co thy ry ae 1 ) \ ‘ HW) c BA ee ay: ‘ p r ‘ \ ofr Wes if CHAPTER XIII GEOLOGY OF THE KENSICO DAM SITE Kensico reservoir at Valhalla, 2 miles north of White Plains, 1s one of the links in the Bronx river aqueduct. -It is to be greatly enlarged and made a very important storage reservoir for the new Catskill system. In line with this plan a new dam is to be built near the old site that will rise 100 feet higher than the present structure. | Extensive investigations’ have been made to determine the charac- ter of rock floor for this massive dam. Sites both above and below the present one have been studied with the question of safety and efficiency and permanence as well as that of economy of construc- tion in view. Involved with this is also the source of suitable stone for its construction. 3 Geological surroundings Glacial drift covers the rock floor of this and neighboring valleys to a depth of 10 to 20 feet. No rock is exposed in the valley bottom at the Kensico site, but at the extremities of the proposed dam the rock floor comes to the surface in small outcrops. The material constituting the drift cover is essentially a loose, somewhat porous till passing into modified types, especially gravels and sands imme- diately south of the ground tested. The character of bed rock at the two extremities and beyond the limits of the dam is easily seen from the outcrops to be Fordham greiss on the east and Manhattan schist on the west. Between, although nothing can be seen, Inwood limestone is found by the borings as was to be expected. No other formations occur, although the Yonkers gneiss, an intrusive in the Fordham at a little greater distance figures prominently in studies of material. The formations are in normal order and are of the usual petro- graphic character. All dip westward at angles that vary from 45 to 65 degrees and have a general strike a little east of north. It is evident that the whole series represents an eroded limb of a simple fold. . 1These explorations have been in direct charge of Mr Wilson Fitch Smith, division engineer, whose headquarters for the Kensico division is at Valhalla, N. Y- Preparations for construction have already been begun. IOI 192 NEW YORK STATE MUSEUM The Inwood limestone occupies about 800 feet of the bottom and eastern margin of the valley, lapping well up on the Fordham gneiss. The drill cores from this formation are unusually sound. The Manhattan schist shows much broken material. There are many crush zones. This condition increases still farther west along the railway near Valhalla station. The Fordham gneiss appears to be sound where it can be seen at the surface. Results of exploration. Many borings have been made. They prove the general structure and succession of formations, making the boundaries definite. They increase the evidences of a rather wide prevalence of weak zones— some of them in the gneisses. And they also indicate a more extensive surface decay than was formerly believed to prevail. The chief problems from the geologic standpoint are connected with the following features: I Extent of surface disintegration 2 Extent and distribution of weak zones 3 Depth of decay and perviousness of rock Surface disintegration. Several borings on ground underlain by Fordham gneiss penetrated material beneath the drift and above bed rock that was interpreted as residuary matter from rock decay. All of this material is of local origin. Later exploration in the form of a deep trench to bed rock has proven that there is an extensive residuary mantle of this sort at the eastern side of the valley below the present dam. In places as much as 30 feet exists. Undoubtedly this material is a remnant of preglacial soil mantle that was in some way protected from removal by the ice. Few places are to be seen in all southeastern New York where there is so much left in place. In most of it the gneissic structure is still preserved, but the decay is so complete that it can be cut and handled like an impure clay. Weak zones. It has been proven that there are weak zones in the gneisses as well as in the other rock formations. In some places the rock is so poor that no core is recovered for distances of 5 to to feet, and in one hole a seam of this kind 20 feet wide appears. In every case, however, the drill passes through the rot- ten material into the opposite wall — indicating a zone of consider- able dip instead of vertical position. This favors the theory that the weaknesses follow the bedding largely and are perhaps due to GEOLOGY OF THE NEW YORK CITY AQUEDUCT 193 difference in the mineral make-up of the beds fully as much as to dynamic disturbances. The walls are generally good. The fragments of core are not much slickensided. In the schist this is probably not as generally true. There are much plainer evidences of crushing movements in the schist. It is a locality where one of the folds, one well developed farther south, is pinched out and there is rather gen- eral crushing of the weaker strata. Depth of decay and perviousness. As deep as borings have gone there is occasional decay and broken ma- terial and streaks that are.pervious. Final location. The condition of bed rock, together with other consid- erations led finally to the selection of a site above the present dam. In general the same features character- ize this site. But the rock condition is somewhat improved. On the whole the new situation is a safer one. caste ocroe 6NCi60 ooras WAIVAL hs 4 FOROHAM too" — cosas Zeozl neg Re +m ct-g the present Kensico dam Geologic cross section across Bronx valley at Vallhalla as indicated by borings on line C2 a short distance below Ufiy TT YY ppp Yy YY Yy Yy Oy YY Ye Fig. 35 ‘Sw > Ps , , baa ? : mils ay ? : : : | ld a ‘ LAS J %. as). aa re Ps ‘ if ee p cha Con” Pee e ' vs iZ . i " . . 7 « LaF, ‘a | mae 2 ay iy! oe aa per ona ee tax Ns Sy e re . 5 was) eels i i wis) ('t 5 ive Rhatiey ae aa ren tee lg ’ ia ‘ we me ha CHAPTER XIV STONE OF THE KENSICO QUARRIES The following quarries in the immediate vicinity of Kensico res- ervoir have been studied in the field: (1) “ Smith quarry,” which is less than a thousand feet east of the southern end of the present reservoir; (2) “ City quarry,” which is on the immediate eastern margin of the reservoir on the east side; (3) “Garden quarry,” which is a new location about 500 feet from the eastern margin about midway; (4) “ Outlet quarry,’ 1500 feet east of the northern extremity of the present reservoir; (5) “ Ferris quarries’ 1000 feet and (6) “Dinnan quarry” 3000 feet farther north. In addition to the field observations a detailed microscopic study was made on specimens of the rock taken from the Garden, Ferris and Dinnan quarries. The question at issue 1s the choice of a rock for the facing and finish of the new Kensico dam. In view of the use to be made of the rock, extreme strength is of only secondary importance. But the questions of abundance, distribution, durability, purity, agreeable appearance and working quality are vital. Types of rocks All of the quarries occur in the broad belt of Precambric gneisses that forms the eastern margin of the reservoir extending northward and southward for many miles. The formation as a whole is very complex. But the basis of it is a black and white banded rock chiefly a metamorphosed sediment, known as the Fordham gneiss in southeastern New York. In it are intrusions of igneous rocks of many varieties and most complicated structure — dykes, bosses, veinlets, stringers etc., sometimes 1n such abundance as to wholly obscure the original type. The most abundant of these are, (a) a rather light colored quite acid rock that is essentially a granite in composition, but has a sufficiently foliate structure to be classed as a gneiss and is the same as the “ Yonkers gneiss” occurring farther south, and (6) a dark rock containing much hornblende and biotite which is in some cases essentially a diorite in composition, but has a marked tendency to schistose structure. The former (a) may be called a granite gneiss and the more massive representatives of the latter (b) may be classed as a dioritic gneiss. In both cases at "4 [Q5 196 NEW YORK STATE MUSEUM times the blending with the original metamorphosed Fordham gneiss is so intimate that absolutely sharp limits can not be drawn. And this last condition may well be designated as a third case (c). The quarries visited represent all three of these cases. Dinnan, Ferris and Outlet quarries represent essentially the “ Yonkers gneiss” type (@) of granite gneiss. Garden quarry represents chiefly (b) the dioritic type of gneiss. City and Smith quarries represent the last case (c), or the mixed and variable type. Field character City quarry. In accord with the above differences in type it is found that large quantities of uniform material for such purpose as is proposed can not be obtained from City quarry. The rock there is badly jointed and is variable to a marked degree. It was not thought promising enough to test in detail. Smith quarry. The conditions of Smith quarry are better but there are similar objections. The amount of uniform material is greater. It would no doubt furnish an abundance of material suit- able for use in the construction of the dam interior, but is not at this point as good a source of facing stone as some of the others to be considered. Outlet quarry. Although this rock is characteristic Yonkers gneiss, it has at this place suffered by weathering a peculiar dis- coloration to such extent as to make it objectionable, both from the standpoint of appearance and perhaps of durability. Garden quarry. There is an abundance of stone at the Garden quarry. It is fairly uniform. It is no doubt good enough from every standpoint of durability. It is well located. It can be quar- ried readily. But it has a very dark color and is undoubtedly less attractive than a light stone for this purpose. There are no objec- tionable structures, except where the strong schistose character 1s developed, and these could be avoided so that with a little selection a fairly uniform stone could be secured. Dinnan quarry. This rock is typical “ Yonkers gneiss.” There is sufficiently large quantity. It is of good quality. It is situated a little over 2 miles from the proposed dam, but is of easy access. The jointing and other structures do not seem to be objec- tionable. It will work somewhat more easily than a true granite because of the gneissic structure and it has a good medium light color. The discolorations do not seem to penetrate deep and the rock shows only slight decay. Plate 28 Photomicrograph of Yonkers gneiss from “Outlet quarry” taken in plain light to show prominence of sutures between the grains indicating the beginning stage of disintegration. Magnified about 30 diameters GEOLOGY OF THE NEW YORK CITY AQUEDUCT 197 Ferris quarries. The “Old Ferris quarry—is “ Yonkers gneiss ” considerably more weathered than the Dinnan. It is con- sidered less promising than the “ New Ferries” quarry which has been explored by the engineers of the Kensico division. The rock of this quarry site is not all of one quality. There are essentially three varietal facies of the Yonkers gneiss type and relationship. One (@) is essentially a granite. It has a coarse grain and shows almost no foliate structure. it has a decidedly massive appearance; but it is not of very great extent. This rock is evidently very closely related to the true Yonkers gneiss into which it passes on all sides through an intermediate variety. This intermediate variety (0) has medium size of grain, is only slightly foliated and passes without sharp limitations on the one side into the granite facies and on the other to true normal Yonkers gneiss. It is not so strikingly massive as the granite, but is more so than the gneiss proper. This rock may be called a gneissoid granite to distinguish it from the other. The true Yonkers (c) gneiss surrounds these two special varie- ties. It is of finer grain than either of the others and is more strongly foliate and is strictly a granite gneiss. Varieties (a) and (6) occur as sort of a lens within the Yonkers gneiss. The extent of the granite as now uncovered at the site is be- lieved to represent its limits. The prospect of enlarging the area will not meet with much success. It is essentially a local develop- ment connected with the differentiation of the parent magma from which all three varieties were derived. It seems to have been the last of the three to solidify, and it has some of the characteristics of certain pegmatite lenses. | Although this is certainly an attractive rock and one against which there is little ground for objection, it is-reasonably certain that a sufficient quantity of this variety can not be obtained here for the whole proposed use. And the prospects are not good for locating another quarry of the same quality. | The gneissoid granite (b) is of greater extent, in fact it will be found to encroach on the present area of the granite. It is as good rock and almost as attractive as the granite. The regular type of Yonkers gneiss such as that represented in the Dinnan quarry can be obtained in almost unlimited quantity, and, with the splendid showing that it makes in further examina- tion, it has come to be considered the best suited to the purposes of dam construction at Kensico. 198 NEW YORK STATE MUSEUM Petrographic character of the rocks This line of investigation is confined to four sets of samples. No. 1 The granite of the New Ferris quarry ‘2 The gneissoid granite of the same quarry 3 The Yonkers gneiss of Dinnan quarry 4 The dioritic gneiss of Garden quarry 1 Granite. The rock is coarse grained and well interlocked. The chief constituents are orthoclase, quartz and microcline. There are but small amounts of dark minerals, and there is not much decay. | Both surface material and the drill core were examined. The deeper material shows a little calcite, that may be original, occur- ring in irregular grains. They do not seem to indicate decay. There is a little kaolin alteration of the feldspars, but not to a serious degree. There are no injurious impurities in the rock such as might cause rapid disintegration or discoloration. The rock is undoubtedly of good grade as to strength, composi- tion and durability. 2 Gneissoid granite (Ferris quarry). The rock is of medium grain, containing quartz, the feldspars and a little mica. There is very little alteration, and no serious decay or injurious constituents. A small amount of sericite and calcite present are not considered of consequence, and as in the case of the granite, the calcite is believed to be original. The grains are intimately interlocked and the rock is certainly of good quality and very similar to the granite proper. 3 Yonkers gneiss (Dinnan quarry). This rock is fine grained, and is composed of quartz, mica and the feldspars among which microcline is very abundant. The condition is good,— very little alteration, close structure, but with a. little more granular appearance than any of the other types. It is a good rock and gives good durability tests. On badly weathered surfaces the Yonkers gneiss breaks up into a granular product like sand long before it decays to earthy matter. This seems to be caused by expansion and contraction of the dif- ferent constituents under changing weather conditions inducing a weakening of the sutures. Sometimes there is very little decay even along these sutures, but as they open slightly they become the channels for moistiire and staining solutions. This makes the boundaries of the grains very well marked in weathered specimens. Plate 29 Photomicrograph of Yonkers gneiss of the type to be used in the new Kensico dam. Dinnan quarries. Magnified 30 diameters _ Photomicrograph of diorite gneiss from “ Garden quarry.” Magnifica- tion 30 diameters. The constituents are hornblende, biotite, feldspars and quartz. GEOLOGY, OF THE NEW “YORK CITY AQUEDUCT 199 Such incipient disintegration is common in the more even grained or granular varieties. The accompanying photomicrograph [pl. 28] is taken in plain light and shows the outlines of the grains due to this cause. 4 Dioritic gneiss (Garden quarry). Rock is of medium grain and with a strong tendency to schistose or foliate structure. The dark grains are hornblende and biotite, the light grains are feldspars and quartz. The rock is fresh, durable and has +9 injurious constituents. It is good enough for the use in ali respects, but has a dark color and is more strongly foliated than any of the others considered. It is evident from these observations that the rocks considered are all of suitable mineralogic character for the purposes of large dam construction. For very large quantities of material, however, it is probable that neither the coarse granite nor the gneissoid granite could be depended upon for uniform supply. The true regular Yonkers gneiss, however, is very abundant, and can be relied upon for indefinite amounts. The dioritic gneiss is also abundant. The immediate region is not capable of furnishing any better rock than those described above. Additional tests Some instructive tests were made by the Board of Water Supply under the direction of Mr J. L. Davis who has charge of the testing laboratories. A few of these applying to the rocks at Kensico are tabulated below. The tests cover: specific gravity, weight per cubic foot, porosity in per cent, ratio of absorption, per cent water absorbed, ratio of drying 24 and 48 hours, retained water pounds per cubic foot 24 and 48 hours. In the accompanying tabulation the terms used are subject to the following limitations as to definition: I Ratio of absorption, sometimes called porosity, “is the ratio of the weight of water absorbed to the dry weight of the stone.” 2 Porosity gives “the actual percentage of the stone which is pore space.” “The difference between the dry and saturated weights of the sample is multiplied by the specific gravity of the rock and the product added to the dry weight. This gives the weight the specimen would have provided it contained no pore spaces. The difference between the dry and saturated weights 200 NEW YORK STATE MUSEUM multiplied by the specific gravity of the rock is then divided by the above computed weight of the poreless specimen. This ratio ex- pressed as a percentage is the actual porosity. Expressed as a formula, the computation is as follows: (Saturated wt. — Dry wt.) S. G. == Porosity.” (Saturated wt. — Dry wt.) S. G. + Dry weight 3 Ratio of drying. An attempt has been made to determine the comparative and actual rates at which the saturated rocks give up the absorbed water under ordinary atmospheric conditions. “ The ratio of drying was computed by dividing the weight of water lost during exposure by total weight absorbed. The weight of re- tained water was computed.” The comparison is most useful in rocks of like petrographic general character. The other terms need no explanation. TABULATION OF TESTS ' o ie} Q, = , : 5 = ES 2 4 a) Bate oF Reames water S| no S ee) 2) @ re) drying pout Ss per | ao] §9 coh De ge Sa cubic feet Sol eel es 5G ONS BQ Name & oO | a6 3 4 — » arm n Oo te © | a5 ¢ 3 3 of | GB G SG S) 3.9 | 0 Opn ip aoe S 24 48 24 |. 48 Chan lS Sea ae x hours | hours} hours | hours a ee Poe reo ee Be ae ‘ec ee) ene x2 Sac OO Granite, Ferris | x] 0.34] 0.77| 2.66| 164.71 | quarry, core No. 461| 2| 0.31| 0.84| 2.65| 164.04 0.26 aie) 52.8 aos aoe ak a ee ee ee | gear age | H Gneissoid granite, 1| 0.3210 0.85H 2.63) 161.03) Ferris quarry, | ©.28|) 67.48] 69.88 .146 -145 core No. 468 | 2) "0n25| tony E) (265126278 | se ee ees |S oo eee ee Yonkers gneiss, I] 0.30] 0.87| 2.64] 163.3 ) | | t | 0.30| 88.16] 88.16 .057 Ob Dinnan quarry 2| 0.39] I.o1| 2.64] 161.0) | ee ee | Fe —— | Dioritic gneiss, 1] 0.42) 0168) 2.83) D754 | Garden quarry, Pi on2rl-62e5 |) 62.5 -137 5137 core No. 459 2| 0.24| 0.68] 2.86) 174.8 } | Gneissoid granite, 1] 0.37| 0.96| 2.63] 162.5 ) Ferris quarry, r | r.08] 86.7 | 88.2 252 -215 surtace 2| ©0.98| 2.50| 2.62| 159.4) Granite, Ferris t| ©.44|) ©.12| 2.63 re teh 0.40] 70.0 | 74.0 207 -180 quarry, surface 2| 0.19| 0.50] 2.71] 167.3 } Mr Davis concludes from a careful analysis and interpretation of these tests that the Yonkers gneiss is of superior durability. CHAPTER XV THE BRYN MAWR SIPHON Geologic conditions as shown by exploration for a proposed pres- sure tunnel Bryn Mawr is a railway station 2 miles northeast of Yonkers. The general features of the vicinity, its topography, succession ot formations and the boundaries are shown on the accompanying sketch map which is largely copied from United States Geological Survey Folio No.83. The Southern aqueduct follows southward along a Manhattan schist ridge until, at a point about a mile northeast of Bryn Mawr, a cross depression of so great width and depth is reached that some special means of crossing has to be devised. Near Bryn Mawr station a gneiss ridge rises and continues south- ward. The proposed line follows this ridge. Explorations have been made as usual by drilling to determine if possible whether or not a bed rock pressure tunnel is practicable. The following questions may be made to cover most of the practical issues of the study: t What formations would the tunnel cut? 2 Which of these would show most questionable ground? 3 What portion of the line is regarded as most critical — whose development would show whether or not a tunnel is practicable? 4 What special conditions are shown by drill borings? 5 What interpretation is to be placed on the peculiar results from hole no. 4 where there has been unusually great difficulty in drilling? 6 What experiences in similar ground have a direct bearing on this case? Formations The formations that would be encountered in the Bryn Mawr siphon are: 1 Manhattan schist (top), the usual micaceous type, also called Hudson schist in United States Geological Survey Folio 83. 2 Inwood limestone (middle), the usual coarsely crystalline dolo- mitic and micaceous type, also called “ Stockbridge dolomite” in tie Folio, same as’ Wuckahoe marble,” same as “Sing Sing marble,’ same as limestone at Kensico dam and also at Croton dam. 201 202 NEW YORK STATE MUSEUM 3 Fordham gneiss (bottom), the usual black and white thinly banded type, a much folded and strongly metamorphosed rock, the oldest of all. 4 Yonkers gneiss, the usual type, gneissoid biotite granite very uniform and granular. This formation is an igneous intrusive that cuts up through the Fordham gneiss and is therefore younger. Whether it is also younger than the limestone and schist is not clear. 5 Quartz veins and lenslike segregations of quartz, also pegma- titic streaks, are occasional occurrences in all of the formations. They are most abundant in the schist, but are seen also in the Ford- ham gneiss. A similar development was encountered in the lime- stone in hole no. 40. 6 Glacial drift, chiefly modified drift, partially stratified sand and gravel, reaching more than 125 feet in depth, covers por- tions of all formations. This last formation (no. 6) is the only one that may be wholly avoided in the tunnel proper. The chief interest lies in its hindrance to exploration and its possible usefulness as a source of sand and gravel supply. | Weakest formation. The Inwood limestone is the most ques- tionable ground. This is believed to be so chiefly because of the greater solubility of the rock, its granular and micaceous character, and the probability that a line of displacement accompanied by some fracturing crosses the siphon line in this formation. If a very excessive amount of shattering occurs in this zone it may have induced a condition of disintegration to such depth as to endanger the tunnel. 3 There are no surface indications of a serious condition at depth for any of the other formations. Critical zone The critical zone is probably not far from the contact between gneiss and limestone. There are two reasons for this opinion. The first is related to the nature of the folding. The formations are squeezed into a close syncline pitching northward. In cross section the strata at any point around the head of this trough dip inward, and, because of the more resistant Fordham gneiss forming the floor of the trough, the drainage and seepage and consequent tendency to decay might be expected to follow along its upper contact. Harts Corner Be ee 29% 4 bbsferry "6 en 8 Oo. + 7 4 oe. Noo Po PLT) ¢ Val ied «ees sa, sal? Cc =—=— “we, “Be xn. Yawr SECTION * anhhetn KS Location map showing by the dotted belts the distribution of Inwood lime- stone in the Hastings-Yonkers district and the position of the Bryn Mawr tunnel section as well as shaft 13 on the New Croton aqueduct with their relations to the limestone belts. Manhattan schist and Ford- ham gneiss occupy the rest of the area. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 203 The second reason is related to the probable later faulting move- ments. It is evident from the map [Folio 83] that the formations in the vicinity of Bryn Mawr are bulged up. One would expect the trough which contains the schist and limestone of Grassy Sprain valley to continue uninterruptedly southwestward and join with Tibbit brook valley. But a cross fold has bulged the formations up so much that for a distance of a mile erosion has removed all oi the formations except the gneiss. Bryn Mawr station is about central on this bulge. Evidence of such a movement is readily seen on the gneiss along the northerly margin where it slopes down toward the limestone. The movement had developed a little-shear- ing and has tilted the minor folds downward toward the north at angles varying from 30° to 80° from the horizontal. This angle becomes somewhat more accentuated as the limestone is approached, and it is believed that it may pass a short distance into the limestone border. There is, however, no great amount of crushing evident in the gneiss and this may hold also in the limestone. The fact that Sprain brook crosses the formations along this northerly margin and flows for 2 miles in a southeasterly direction may indicate a still later movement, probably faulting. There is no surface evidence of it except the abnormal course of the creek. But, if there is such a fault, it also crosses the siphon line in the same zone, i. e. in the vicinity of the limestone-gneiss contact, not far from the location of the present course of the brook. Therefore it seems reasonable to conclude that the critical zone is near the contact, probably on the limestone side, and in the vicinity of the present course of Sprain brook. It is also probably cut deepest here by erosion. If this zone is in good enough condition to stand tunneling the rest of the line ought to be. Conditions indicated by borings ' All rock formations stand very steep. They vary from 80° to go°. This means that very few beds can be explored by one hole, and that any weakness or crevice is likely to make a showing in excess of its true proportions. The cores show considerable crushing. Some of the fractures are not healed, although weathering from circulation is not present on all of them. The micaceous layers are most affected by circula- tion. Some beds of this variety are considerably weakened even at depths of over 200 feet. Occasional seams have been encountered that give no core at all for several (even 20 or 30) feet. But the 204 NEW YORK STATE MUSEUM greater proportion of the recovered pieces are comparatively solid even where the total percentage of saving is very low. It is evi- dent that some of the core, a considerable percentage, has been ground to pieces in the process of boring. This is especially notice- able at hole no. 40. Hole no. 40. Much trouble ee been met in this hole. A careful analysis of the record and core and the behavior of the drill is interpreted as follows: 1 Partially assorted drift, chiefly sand and gravel was penetrated for 125, fect. 2 Limestone bed rock of fairly sound sees was struck at about 125 feet (about el. —40). . 3 The casing that was put down to shut out the sand failed to reach solid rock, and this permitted a continual supply of pebbles and sand to run into the hole and obstruct the work with each pull up. The presence of these pebbles was also instrumental in grinding the core to pieces, and this accounts chiefly for the low saving. 4 After this opening was plugged up with cement, the drilling was continued successfully until a somewhat broken quartz vein was encountered and this has been followed for about 35 feet. Its broken condition afforded another opportunity for fragments to fall into the hole, and on top of the drill, bringing the work for a second time to a standstill. It is certain also that the drift pebbles still fall in. As the formation stands vertical here it is not surprising that any feature should show an apparent extent quite out of proportion to the real value. The quartz vein is probably of no great breadth. Small seams containing mud may also be followed 15 or 20 feet and still be of no great significance in the formation as a whole. The rock fragments (core) recovered in this hole are fairly sound. 5 In spite of the many delays and difficulties of this hole, it is apparent that the general rock formation is not responsible for it all. The failure to reach solid rock contact with the casing has been the cause of part of it. Later the penetration of a rather rare quartz vein, a thing that would not often be found in the limestone, has added to the trouble. Both of these causes are so rare that they may almost be given the value of accidents. But the last 100 feet or more of the hole, from depth 225 feet to 335 feet, shows an unusually questionable condition. Only a few rock fragments are saved and they include limestone and quartz vein matter. The rest is wholly disintegration sand of rather com- plex composition but carrying very much mica. This is all wash GEOLOGY OF THE NEW YORK CITY AQUEDUCT +, yA % aw ,, t 0 NR ROE RO Ls L Ne 0 a SSN E AX SS ech 2 AY SOR ANY 3 Nt Xe NY BOA AND AY ERNE NAA y x RYN. ia O) (NRE TAR x ee a RAINY ICN 43 SONG q on 8 b, NS RONONE 0, AWN = Ee ane See Z SS LE. 7 SEEKS SS KS Ss Se, > KRAI EZ 3 Cis 2 <) 5 C ES, Se ES ES Ss ee EAA EZ ZB g Zz tS O CJ e SZ a PSS ee ASS ES 1S Zee CGSocesss LESS co 6 s g id 2 g SZ Z FSH peed SATS“ PASS LEE SA SSE c3 sss Bass aa ZA v c CACSe ce Zs EEA > b ZS Z Z aa VS > Z a5 g SES | RW SM proreetes T_ RR Lie NIN aaa c HOUT |EXPLO! TL 7 F : o re 2 S z 3 $ x 3 ® ; YI ‘ - r ° N aa i = ° 3 eee | ° ang ° ° Zo ° 25 ae i saainite dae Pa (BEE FEE A a) Le GEOLOGIC SECTION AT BRYN MAWR “NOLLWLE line from north to south showing the geologic structure interpreted from drill borings - Fig. 36! Section along the aqueduct 205 206 NEW YORK STATE MUSEUM material except one sample, which is a “dry sample” and is still more strongly micaceous. Borings nos. 40, 45 and 46 are ail within the zone that was con- sidered, from surface indications, to be likely to carry the deepest gorge and to show the weakest rock. Because of the heavy drift cover (more than a hundred feet) it is manifestly impossible to locate the weakest zone more closely or judge of its exact condi- tion except by borings. Hole no. 42 at station 634 +28, penetrates 82.4 feet of drift and reaches bed rock at about elevation 21 feet A. T. The rock is good, substantial, coarsely crystalline limestone. It shows as sound con- dition as can be expected in this formation even under the most favorable situations. Hole no. 46 at station 644+-77.4 is just south of the brook. It penetrates 72 feet of drift and reaches bed rock at elevation 14 feet A.T. The rock is Fordham gneiss of typical sort and in per- fectly good condition. There is no question about the soundness of the rock from this point southward. Hole no. 45 at station 643+ 52.5, 125 feet north of hole no. 46 penetrates drift for about 150 feet (possibly a few feet less, 145 feet). This drift cover is interpreted as mostly sand (modified drift) to 115 feet and a boulder bed from 115 to 143 feet. After the true ledge is reached it is sound and shows no unusual or ques- tionable conditions. It is Fordham gneiss. Interpretation 1 Weak zone. There is little doubt that this last 100 feet of hole no. 40 is in the decayed weak zone that was expected to de- velop in the vicinity of the contact between the gneiss and the lime- stone. It would be expected to pitch northward along the floor of gneiss and extend beneath the southerly extremity of limestone at this point [see fig. 36]. 2 Contact. Hole no. 40 cuts limestone, hole no. 45 cuts only gneiss, therefore the formational contact lies somewhere in this 177-foot space. 3 Position of old channel. Bed rock surface is lowest at hole no. 45. But since the rock itself is sound gneiss, it is not believed to represent the lowest possible point. This is still more certain because of the fact that the pitch is northward so that this becomes a dip slope on which the preglacial stream could glide against the edges of the limestone beds [see diagram], and because the condi- GEOLOGY OF THE NEW YORK CITY AQUEDUCT 207 tion of the rock a little farther north (at hole no. 40) shows that these limestone beds are actually much weaker than the gneiss. Therefore the deepest portion of the buried channel is to be expected between holes no. 40 and no. 45, and probably nearest to hole no. 4o. 4 Depth of old channel. How deep the buried channel may be can not be accurately estimated. But if the same dip slope as is shown by the rock surface from hole no. 46 to no. 45 prevails northward toward hole no. 40, a depth somewhat below —100 feet may reasonably be expected. In the absence of data bearing upon the depth of other portions of this ancient channel or of the lower Bronx river with which it must have been connected, it is impossible to estimate more closely. 5 Interpretation of hole no. 40. There is so little rock actually saved from the more than 200 feet of possible core on this hole that its real character is very obscure. There are three possible explanations for the condition found in the last 100 feet. a The drill may have followed a large mud seam. b The material may be only residuary rotten limestone still wholly above the gneiss. c The actual contact may have been penetrated and a part of this rotten material may be decayed gneiss within a crush zone. The difficulty in drawing absolute conclusions is increased by the fact that matter falling in from above has been a continued source of trouble and is more or less mixed with the rock material of lower points. Therefore, the fact that the sand taken from the lowest points, 335 feet, is silicious instead of calcareous, may not prove satisfactorily that the rock at that point is wholly silicious. It is worth noting, however, that the harder rock in the upper portion of the hole was in places much crushed and that mud seams were encountered before reaching this last 100 feet. It is also worth noting that the same dip slope of rock surface as prevails between holes no. 46 and no. 45 if continued northward to hole no. 40, would cut that hole a considerable distance (75 feet) above its bottom. In view of all the conditions, therefore, it is judged that there is a crush zone here, that hole no. 40 penetrates it, that it 1s badly de- cayed, that the plane of the crush zone dips steeply northward and cuts both limestone and gneiss, that a tunnel at about —300 feet would cut this zone south of station 640 and north of station 642, and that all other portions of the line are in comparatively satisfac- 208 ; NEW YORK STATE MUSEUM tory condition. This zone for a hundred feet is likely to be wet, weak, and would require extra precautions and additional expense in construction. 6 Evidence of faulting. Whichever interpretation of hole no. 40 is taken is in support of some displacement in the nature of faulting between holes no. 40 and no. 45. If the gneiss rock floor is not reached in hole no. 40, then the greater northward slope of © it from hole no. 45 to no. 40 than is shown from no. 46 to no. 45 indicates a downward movement. If on the other hand, the iden- tity of the formation in the lower part of hole no. 40 be considered undetermined, and its condition attributed to decay in a crush zone, the presence of the crush zone itself indicates. movement of a fault nature. Conclusions as to character of the crossing In considering the geological conditions as a factor in the prob- lem of practicability of a tunnel, it is necessary to note the follow- ing points: 1 In view of the fact that the deepest point in the ancient chan- nel is not yet found, and that it will probably go below —I00 feet, it would be necessary to figure on a tunnel grade down well toward —300 feet. 2 It would be necessary to figure on a wet and weak zone of at least 100 feet along the tunnel and a more expensive construction at that point. 3 The ground at such depth south of station 642 is unusually sound. The ground north of station 636 may be counted good. The ground between 636 and 640 may be considered fair, and the ground from 640 to 642+, troublesome, containing the chief ele- ments of uncertainty. Fig. 36, which is a geologic section along the line at this point, shows the distribution of these features drawn to scale. . CHAPTER XVI A STUDY OF SHAFT 13 AND VICINITY ON THE NEW CROTON AQUEDUCT [See outline location map, pl. 30] There has been reference made occasionally in connection with the Bryn Mawr explorations, as well as others, to the remarkable piece of bad ground encountered in 1885 on the New Croton aque- duct near Woodlawn in the Saw Mill valley. This experience has been the source of much misgiving. Because of its evident im- portance and close relationship to conditions that may exist in the same formation at points on the Catskill line, an examination of this ground was made for the purpose of comparison. The mean- ing of that case and its bearing on the Bryn Mawr questions aze given below: z Engineer’s records This ground and its remarkable behavior is describéd by Mr J. P. Carson in the Transactions of the American Institute of Mining Engineers, September 1890, pages 705-16 and 732-52. A description is also given in Wegman’s Water Supply of the City of New York, 1658-to 1895, on page 152. From Mr Wegman’s report is taken the following: The south heading was started from this shaft on June 1, 1885. It advanced at the rate of about 80 feet per month for 392 feet through good limestone rock (dolomite), which then became softer. On December 9, 1885, when the heading had reached a point 407 feet from the shaft a fissure was encountered from which about 100 cubic yards of decomposed limestone clay, sand and dirty water poured into the tunnel, partly filling it for a distance of 125) feet. After three days delay, when only clear water was flowing into the tunnel, the fissure was plugged with straw. The heading was ad- vanced 20 feet further until on December 22, 1885, an outpour three times greater than the first occurred, covering everything in the heading out of sight * * * borings were made on the surface with a diamond drill to determine the extent of the soft ground in front of the tunnel. It was found to lie in a pocket in the rock, 209 210 NEW YORK STATE MUSEUM which had a length of 110 feet on the axis of the tunnel and ex- tended for a short distance below the invert of the conduit. The soft material, consisting of sand, gravel, clay and decomposed rock had a depth of about 160 feet from the surface to the top of the tunnel. It exerted such a pressure against the timber bulkhead that the 24-inch oak logs used as “ rakers”’ (braces) became crushed in 24 hours and had to be continually renewed. The chief points of present interest are that the tunnel, at a depth of about 160 feet from the surface, and after passing through sev- eral hundred feet (407 feet) of good dolomite, came into rotten rock and soft ground 110 feet across on the line. It was so soft that it ran into the tunnel in great quantities and exerted such pressure as to make progress in it a very troublesome and costly matter, taking “ 60 weeks to advance the tunnel 85 feet’ and costing “ $539 per foot.” The material caved in so freely as to form a pit on the surface. Statement of geologic conditions It is not possible to interpret the conditions at this locality as fully as one would wish because of the vagueness of some of the statements, but the following facts and explanation are essentially COELECE : 1 The rock is the Inwood limestone, the same kind and same general conditions as all of the limestone belts that occur in the region of the Southern aqueduct. 2 The soft ground penetrated at the point in question — 407 feet south of shaft 13 — called in the Carson report and others “a fis- sure’ or “ pocket,” etc., is in reality a fault crush zone. The fault plane probably dips steeply southeast and strikes n. 50° e. cutting the tunnel line at an angle of something like 20°. 3 The point is well up on the side of the valley more than a hundred feet above Saw Mill river, and the strike of the fault zone in its southwesterly extension cuts into the lower portion of the valley, so that underground circulation would be encouraged along the zone in this direction. 4 The limestone outcrops very near by on the west side of the line and the Manhattan schist occurs near by on the east. The atti- tude of the beds is such as to indicate a fault of the thrust type, The accompanying figure illustrates this relationship in a cross sec- tion at right angles to the axis of the tunnel [see fig. 37]. GEOLOGY OF THE NEW YORK CITY AQUEDUCT ZIi1 Crush Zone Fig. 37 Sketch of the geologic structure at shaft 13 on the New Croton aqueduct. Interpreted from field observations 5 It would appear probable that this zone was penetrated at the worst possible level, i. ec. near enough to its wholly decayed upper part to furnish no resistance at al! to the overlying sand and gravel, and not deep enough to reach the more substantial (although prob- ably crushed) rock that may reasonably be expected to prevail at no very much greater depth. The chief point is that the weak spot has a reason and is not an accidental thing that might be expected just anywhere. But it must be admitted, in spite of this fact, that a casual examination of the iocality would not make one suspicious of its existence, and it is surprising that the spot could have caused so much trouble. From the above it will be seen that in several respects the Bryn Mawr case is somewhat similar to this. They both indicate fault- ing; they are in the same type of rock; they both show or indicate caving tendencies. On the other hand, there are certain elements of difference some of which are capable of very materially modifying any conclusion that might be based upon the simple facts of likeness. For exam- ple — it should be expected (1) that the fault movement at shaft 13 would be the greater because of lying in the more prominent lines of such displacement of the region, (2) being a thrust movement, the crush effect is probably more prominent at shaft 13 than at Bryn Mawr, (3) occurring at greater elevation above probable cir- culation outlet, the opportunity at shaft 13 for extensive and rather deep decay is the greater, (4) being cut so near the surface (160 feet), its condition there is not necessarily a reliable guide to the seriousness of decay at a greater depth. 212 NEW YORK STATE MUSEUM Comparison of Bryn Mawr and shaft 13 The following statements embody an opinion on the points raised or suggested in connection with a reference to the New Croton difficulties at shaft 1 3. The items are therefore treated by compari- son or contrast so far as possible: 1 Type of rock. The rock explored at the Bryn Mawr siphon is the same formation as that in the Saw Mill valley cut by the New Croton aqueduct, i. e. the Inwood limestone — sometimes called “Stockbridge dolomite.” It is the same also as the other large limestone belts in Westchester county. There are occasional small strips of limestone of another type, but its behavior could not be very different. 2 Soft material. “Is any material of this sort” (like that in the New Croton tunnel near shaft 13) “likely to be encountered either in the crushed zone at boring 40 or elsewhere in the lime- stone belt?” It is sure to be encountered, especially near hole 40, if that zone is cut shallow. The behavior of the lower portion of this hole is very similar to the described case near shaft 13. The only prob- ability of avoiding it lies in placing the tunnel deep enough to cut more substantial rock. The single hole upon which all this argu- ment is based can scarcely be considered a thorough enough ex- ploration to build up a quantitative statement as to depth or width. There is no evidence, either on surface or in the exploration holes, of any other such zone on this line. 3 Depth and extent. Under the circumstances, the increased depth makes it less probable that so much ground of like behavior would be found. Again, it is not likely that precisely the same conditions would so effectually halt operations or be considered so nearly insurmountable at this time. One of the many serious objections is that the tunnel would have little strength or resist- ance to a bursting pressure. It must be admitted that if caving ground were penetrated it would prove very difficult to handle with the gravel cover at the depths now considered, 1. e. 300 feet or more below the surface. : 4 Water. “ What are the probabilities in regard to the quan- tity of water to be met in the crushed zone near boring 40? Can any limit be set which it would be extremely improbable that the inflow would exceed, on account of the topography of the country and the nature of the overlying materials?” There is likely to be much water. Nearly all of the overlying GEOLOGY OF THE NEW YORK CITY AQUEDUCT 213 drift is sand and gravel that is probably saturated and in such con- dition as to permit easy flow to any lower outlet. It may readily carry 8-10 quarts of water to the cubic foot or about 2 gallons. The area covered by such deposits is about 2500 feet long on the southerly base along the creek and at this margin is approximately 150 feet deep. The northerly margin is variable and reduces in places to o feet in thickness. It may, however, really represent 500,000,000 cubic feet of this gravelly material holding 1,000,- 000,000 gallons of water as a nearly permanent supply. This overlying material is necessarily a menace of no mean pro- portions. Every crevice or crush zone remaining unhealed will have water and plenty of it, the inflow being limited only by the size of the cracks and their abundance untii the reservoir should be drained. There is no hardpan bottom to act as a dam. Outside additions to this permanent supply are confined to that received from rain and the stream. The rainfall on the area and immediately available as addition to the underground supply in the lower sands, together with the stream flow, which would probably sink into the sands, if an attempt to drain the underground supply were made, may be expected to furnish additional water at a pos- sible rate of 2500 gallons per minute. How much of all this is available at tunnel level depends wholly upon the openness of structure in the rock. There is nothing else to materially control the permanent and additional supply. There is evidence in hole 40 of considerable crushing. That means capacity for water circulation, but how much no one can tell. There is also much rotten rock in the same hole. This means that circulation has been easy and effective, but how much now no one can tell. The single hole (no. 40) in the absence of any other corroborative data is not sufficient to base more elaborate or precise quantitative estimates upon. 5 Solubility. What is “the nature of the limestone with reference to its resistance to solution?” This limestone is, as all limestones are, more easily attacked by circulating water than most other rock types [see Rondout Valley]. The Inwood limestone such as occurs at Bryn Mawr is crystalline, often contains much mica and then is inclined to be foliated in structure, and it prevailingly stands steeply inclined. Because of these features in which it differs from the Rondout Valley lime- stones, it is likely to be more generally affected by decay along the zones permitting circulation than any of the Rondout Valley types. 214 NEW YORK STATE MUSEUM The Rondout Valley limestones are affected along joint planes, but the effect is almost wholly confined to a simple enlargement of these crevices. In the Inwood an additional effect is the weakening of the sutures or bond between the individual granules resulting in a tendency to weaken the whole mass as far as there is much pene- tration of seeping water. It would have less tendency to produce openings or caves, but greater tendency to produce a rock that would crumble in the hand or that would gradually assume the con- dition of a lime sand or a micaceous mud. As to the effect of water from the aqueduct on fresh portions of this rock, it is certain that the rock would be attacked wherever exposed to direct action. Its method of attack is by solution, and the rate of attack may safely be reckoned as not materially different from that assumed or being established by experiment and expert- ence on the Rondout Valley types. In the final consideration of the difficulties at Bryn Mawr the engineers have decided to abandon the tunnel plan. It is probable therefore that no additional explorations of direct bearing on the problems of this ground will be made. CHAPTER XVII GEOLOGICAL CONDITIONS AFFECTING THE LOCATION OF DELIVERY CONDUITS IN NEW YORK CITY Hill View reservoir is the terminus of the Southern aqueduct. The Catskill water is to be delivered at this point, just north of the New York city line on the Yonkers side, at an elevation of 295 feet. From this reservoir the water is to be distributed by an inde- pendent system of conduits to the principal centers of consumption in lower Manhattan and Brooklyn. It is believed that distribution can be most economically made and the system be most permanently established by constructing the main trunk distributaries as tunnels in solid bed ‘rock at con- siderable depth below all surface disturbances. Preliminary investigations have been carried on by Headquarters department, Mr Alfred D. Flinn, department engineer, beginning in 1908. As the active work of exploration was entered upon Mr William W. Brush, department engineer, was assigned to this special division of the department’s work and most of the preliminary ex- ploration borings were planned and finished under his immediate supervision. With the resignation of Mr Brush to take the post of deputy chief engineer in the Department of Water Supply, Gas and Electricity, Mr Walter E. Spear, department engineer, was secured to continue the difficult work of finishing explorations and preparing for construction. Studies of conditions affecting such a system and explorations designed tc test the ground in line with these studies have been made. The work thus far done in an exploratory way has been © confined to one main distributary. Section A. Preliminary geological study As a preliminary step toward the systematic study of local con- ditions affecting possible conduits, trial lines were laid out on the 1Few engineering enterprises, probably, have been planned with so care- ful regard for all known geologic conditions. The geologist and the en- gineer worked alternately on the same problems until, in the opinion of both, the best possible line was selected. It is the writer’s belief that so sys- tematic a method has seldom if ever been carried out in engineering work of this kind. On this account, and in part to illustrate some of the pre- liminary stages in such work, many of the original facts and arguments and suggestions are given without change in the following discussion. 215 216 NEW YORK STATE MUSEUM city map from Hill View reservoir to Brooklyn by three different routes. So far as the topography and city development and other engineering considerations could be forseen either route could be used. Studies of all kinds were expected to indicate which would be the most favorable and whether or not it might be advisable to shift even the best one to still more favorable ground. These are shown on the accompanying map which also covers the local geology of the immediate vicinity of the lines [see pl. 32]. General questions When the problem of the practicability of a rock tunnel for distribution conduits was first studied, several general questions were raised which indicate the lines of investigation followed. 1 What is the character of the rock along the projected conduit lines shown at the depths required for such tunnels? 2 Will the rock at moderate depths be such as to permit success- ful and economical construction of tunnels to be used under the hydraulic pressure due to Hill View reservoir? 3 Does the character of rock in the vicinity of the lines vary sufficiently to materially affect the cost of a tunnel if the lines be shifted approximately 1000 feet either way from those shown on the original map as trial lines? 4 Are the suggested locations of conduit lines adapted from a geological viewpoint to the construction of pressure tunnel con- duits, and, if not, what changes in these lines would be advisable? 5 Is the thickness of rock covering sufficient at all points to obviate trouble from open seams and disturbed surface rock? 6 What borings and other field investigations should be under- taken to determine the practicability of construction of pressure tunnels along the lines suggested? In line with this series of questions a thorough geological investi- gation was begun, the chief conclusions of which are given below. Geological formations There are six local formations of sufficient permanence and in- dividuality of character and of sufficient areal importance to be treated as units in this study. These are described in some detail in part 1, but for convenience are briefly listed as follows: 1 Glacial and postglacial deposits of boulders, clay and sand, with silt beneath the rivers. Plate +31 oe ~~ “roe iL Parr e, Reproduced from a model p of New York city and environs. A relief ma by Howell. ”) ? “f ei GEOLOGY OF THE NEW YORK CITY AQUEDUCT 217 2 Manhattan schist, the most abundant formation, chiefly mica schist with very subordinate hornblende schists, and usually with abundant pegmatite lenses and veiis. 2, The Inwood limestone, a white, dolomitic marble when fresh, which shades into impure, micaceous varieties. 4 The Fordham gneiss, varying from a thinly schistose or quartzose rock to a strongly banded or a very massive and much contorted gneiss. The oldest formation of the district. 5 The Yonkers gneiss, an original intrusive granite, now squeezed into a gneiss. Younger than the original Fordham. 6 The Ravenswood grano-diorite or as it might be called in engineering practice, granite; an original, intrusive rock now some- what gneissoid from pressure. Younger than the original Fordham. The Manhattan schist, the Inwood limestone and the Fordham gueiss are cut by veins or dikes of coarsely crystalline granite, technically called pegmatite. They are of irregular distribution and do not affect the tunneling operations one way or another. All the formations older than the glacial drift have been com- pressed into a series of northeast and southwest folds, and all have as a rule a steep or almost vertical dip. The axes of the folds are not horizontal, but usually pitch downward to the south at low angles. Erosion has developed a series of ridges trending north- east and southwest. The limestone being a softer and more easily eroded rock, almost always underlies the valleys or flats and the river channels. It is certain also that there is some faulting. Rock at depth The distribution of geological formations along the proposed lines has been shown on the accompanying map [pl. 32]. In gen- eral the kind of rock at tunnel depth will be the same as at the surface as indicated on the map for each point. Such error as there is, arises from two causes: (a) Uncertainty as to the exact location of some of the contact lines between two formations (usually due to drift cover), and (0) dip and pitch of the strata. - In the first case (a) where the drift is particularly heavy, it is sometimes impossible to fix a contact line accurately from surface features alone. In the second case (>) it must be appreciated that nearly all of the formations dip eastward at a very steep angle, so that a form- ation would usually be found to extend a little further east at depth than at.the surface. And also all formations pitch southward, so 218 NEW YORK STATE MUSEUM that they would be found to extend considerably farther south at depth than their surface outcrops. This angle of pitch is from ne” £0.30". In nearly all these cases, however, the obscurity of the actual surface boundaries is as great a source of uncertainty as the effect of dip and pitch, so that the boundaries as mapped may be con- sidered sufficiently accurate for this comparative study of the lines. It is worth noting that the rock at the proposed depths of tunnels would be, as a rule, more substantial than at the surface. But there are several places on all of the lines where the exact condition is unknown at the surface as well as at depth. The chief points of this character will be noted in a later paragraph. Comparison of lines* A comparison of the three lines submitted as the basis of ex- amination — (a) the westerly one, (b) the central one, (c) the easterly one [see accompanying map, pl. 32], as to rock formations likely to be cut by them, furnishes the following figures: Line A. Going southward from Hill View reservow Feet 6200 Yonkers gneiss — good rock 1 400 Fordham gneiss 1400 Probably largely Inwood limestone with one weak zone (at Van Cortlandt lake) 5 600 Fordham gneiss — good rock 2400 Near contact with limestone, probably in gneiss 1600 Crossing Harlem river — Inwood limestone 4000 Inwood limestone — probably fairly good rock 800 Inwood limestone — probably containing bad zone to Speedway 16 400 Manhattan schist (to 135th st.) 2000 Along contact between schist and limestone 4200 Inwood limestone with one weak zone (to s. end of Morningside Park) 1The statements of quality and extent of certain formations and zones are capable of some modification as exploratory work progresses. Some of these are noted in later sections of this report under special headings, such as The Lower East Side, and The East River-Brooklyn. section. For the present purpose, as showing the development of the geologic basis of the project it seems preferable to leave the accompanying comparisons in their original form as presented to the board. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 219 12 800 Manhattan schist probably good quality (to s. end of Cen- tral Park) 21000 From Central Park to East river —no outcrops — mostly Manhattan schists at tunnel depth. Condition largely conjectural'— probably mostly good rock with occasional weak zones 6000 Manhattan island to City Hall, Brooklyn. Containing an unknown! zone in the East river and unknown quality of rock in Brooklyn. Summary of Line A Feet 6 200 Yonkers gneiss 7000 Fordham gneiss 2400 Contact (probably in gneiss) 12000 Inwood limestone 2000 Contact (probably in ieseone) 29 200 Manhattan schist (good) 21 000 Estimated Manhattan schist (fair) 6000 Almost unknown 85 800 total Line B. Going southward from Hill View reservoir Feet 8000 Yonkers gneiss — good quality 13 000 Fordham gneiss — good quality 6 800 Inwood limestone, probably mostly in fair condition, except at two points (to Cromwell av.) 6 600 Inwood limestone, unknown condition, but probably largely poor (to Harlem river) 600 Inwood limestone — unknown condition (Harlem river) 4600 Inwood limestone — unknown condition — probably fair (to Mt Morris Park) 800 Manhattan schist. good 800 Probably Manhattan schist — unknown 2800 Inwood limestone — unknown condition — probably at least one bad zone (to 106th st.) 12000 Manhattan schist along Central Park — good 1 Explorations since conducted by the Board of Water Supply have proven the quality and character of the rock floor at these places. For the revised statement on these sections see the special discussions. 220 Feet 8 600 I4 000 6 000 Feet 8 000 13 000 2I 400 12 800 23 400 6 000 84 600 Feet 6 000 17 400 5 000 9 800 1 800 600 6 400 I 000 I 200 I 800 I OOO I 000 7 O00 2 800 18 400 NEW YORK STATE MUSEUM To Broadway — Manhattan schist (little known except from tunnels already made) To East river, probobly Manhattan schist (same as line A) Manhattan island to City Hall, Brooklyn — uncertain con- dition (same as on line A) SUMMARY OF LINE B Yonkers gneiss — good quality Fordham gneiss — good quality Inwood limestone — variable quality Manhattan schist — good quality Estimated Manhattan schist — fair Almost unknown total Line C. Going south from Hill View reservoir Yonkers gneiss — good rock To Webster av.— Fordham gneiss — good rock Along contact between limestone and gneiss To 138th st— Inwood limestone with probably two bad zones To Bronx kills-—along contact between limestone and gneiss — uncertain quality Across Bronx kills— mostly in limestone containing a fault zone — probably bad ground Crossing Randall's and Ward's islands and Little Hell Gate. Nearly all is Manhattan schist of good quality Crossing Hell Gate —. Inwood limestone Crossing Hell Gate — Fordham gneiss of good quality Astoria point — probably Fordham gneiss of good quality Crossing another limestone belt To Vernon av.— Fordham gneiss of unknown quality con- taining one fault zone To Nott av.— Ravenswood grano-diorite — good rock To Borden av.— Probably Ravenswood grano-diorite. To Fort Greene Park Brooklyn — almost wholly unknown but contains probably 5000 or 6000 feet of poor ground GEOLOGY OF THE NEW YORK CITY AQUEDUCT 221 SUMMARY OF LINE C ~ Feet 6000 Yonkers gneiss — good quality 17 400 Fordham gneiss — good quality 6 800 Along contact between limestone and gneiss (questionable) 12400 Inwood limestone — with several bad zones 6 400 Manhattan schist — probably good quality 3.000 Fordham gneiss -— probably good quality 1000 Fordham gneiss — unknown quality 9 800 Ravenswood grano-diorite — mostly very good rock 18 400 Almost wholly unknown 81 200 total Tabulated summary — Types of rock formations LINE A (WEST) LINE B (CENTRAL) LINE C (EAST) Per Per Per Feet cent Feet cent Feet cent Monlrense oneiss: sone. i vie-c8 6200:5 7(7 <2) 8000, “(9 4) 6000 (7.3) Bordham (\etieiss 22.25 625.24 7000. (S21), 13000 (45.3))) 21400 (26:3) Gantachn zones iss. ae ae A 400. (5:1) O (O)i a eGrsco!, (853) Inwoods limestone i). 3..42: PAOGOs C14.) . 21 400 (25.3) 12400 (15.2) Manhattan Schist sos ...c55 « FO 200 (56.5) 36200 (42.6) 6400. (7.8) Ravenswood grano-diorite . ) (0) O (0) 9800 (12.0) Olay cc coh oe oe Sow sss 6000 (7.0) 6000 (7.0)- 18400 (2.6) Motawlenetiy we). faves: LS5 O00 2 See oc S41 G00» 255. ie S200" Geae fs: Summary of quality LINE A LINE B LINE C Per Per Per ; Feet cent Feet cent Feet cent Goad sock, 1st; erade. 552+. 42400 (49.4) 33800 (40.0) 39800 (49.0) Probably, air, 2d’ erade;.:. 30800 (35:0) 34800 (4r:t) 13600 (16.7) Probably poor, 4d strade.... 6600. (7.7) too00 (11.8) 9400: (TY.6) MIMOSH MNKHOWIE ook... --< 6000 8(7.0) 6,000" 3) (751) ae. te 700.” (22:7) 85800 100.0 84600 100.0 81200 100.0 Argument on choice of line In judging the quality of rock and its suitability for this con- duit the factors of most weight are the same as those repeatedly mentioned in connection with other portions of the Catskill aque- duct line. That is, in brief, that the harder crystalline rocks of the Fordham gneiss and) Manhattan schist types wherever known to be 222 NEW YORK STATE MUSEUM free from fault crushing and surficial weathering are the best variety ; that the more heavily buried areas of these rocks, together with those limestone areas that are known to be the most substan- tial of its class, should be regarded as fair or second grade; that the more obscure areas of limestone and all portions crossing faults or rivers or crush zones in any rock must be regarded as poor or third grade. This rating is based wholly on rock char- acter and without any consideration of cost of construction. From the above it is clear that line A has more “first grade ” rock than either B or C and less “ third grade” ground. Line C has three times as much “unknown” ground as either B or C and less “ first’ and “ second grade ” rock. In other words, the three lines are estimated: Se i ae a pie oh Birst rade ‘rocky ..u Sie Pee ee 49.4 40.0 49.0 mecond Sradewocks) S22 le mens ae oe 35.9 AI.1 16.7 First and second grades together....... Obes 81.0 O527 Mihind grade cocliis: eC e) ee: 7.7 11.8 LAG Wrknown’ erounde enn a Beles. aks 720 Het 22.7 In addition to these differences of quality, it appears from a study of the areal geology along the respective lines that a tunnel would pass across limestone contacts from one formation to an- other six times on line A, four times on line B, and seven times on line C. These may all be considered points of probable weakness. All of the lines cross belts of well known weakness believed to represent fault zones. Line A crosses three such zones, line B crosses two, and line C crosses at least three. Furthermore, all of the lines cut limestone for greater distances than seems desirable or necessary. The weakest ground and the most uncertain quality of ground that can be mapped falls within the limestone areas. In this respect line A with 13.9% of limestone ground is preferable to line B, with 25.3% or line C, with 15.29. From the above it is apparent that line C is least defensible. Line A has some advantage over both of the others, especially in quantity of first grade rock quantity of first and second grade together, low amount of the known poorest grade and small extent of the so called “unknown” ground. The chief advantage of line A over line B lies in its much smaller limestone area (12,000 feet vs. 21,400 feet or 13.9% VS. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 223 25.3%), and the chief advantage of line A over line C lies in its much smaller amount of “unknown” ground (6000 feet vs. 18,400 feet or 7.0% vs. 22.6%). On these grounds line A is the least ob- jectionable of the three lines proposed. But it is also clear from an examination of the field, as is shown on the accompanying map [pl. 32], that it is possible to avoid some of these objectionable features or certain parts of them and materially improve the figures by shifting the line to a sort of com- promise position between line A and line B. This compromise line, or the trial lines from which the final tunnel line may result, should follow as closely as possible the gneiss and schist ridges and should avoid the limestone areas and known weak zones wher- ever possible. Depth of tunnel The rock formations in general at the required depths are no more objectionable on Manhattan island or in The Bronx than at other localities on the Southern aqueduct. There are weak places and crush zones to be crossed and some of them can not be avoided by any possible manipulation of the line, but these most question- able spots constitute but a small proportion of the whole distance. The depth most suitable must depend chiefly upon the depth neces- sary at the worst spots. Comparative cost of construction if lines are shifted The question is best answered by reference to the geological map. It will be noted especially that the belts of the different rock forma- tions are usually narrow, and that they run nearly parallel to the average direction of the lines. Therefore a shift of line to no great distance would at many points place it within an entirely different formation. It is also notable that all of the lines run along or near the contacts between formations for long distances. At such points a very small shift would wholly change the type of rock and rock quality. Some shifting is desirable. In general it may be assumed that the limestone belts would be easiest and cheapest to penetrate wherever they are fairly substan- tial, but they undoubtedly also contain the greater proportion of weak and troublesome ground and must be considered least desir- able from the standpoint of maintenance and durability. The gneisses are probably most expensive to penetrate and the schists, medium. Both are more expensive than limestone but both are more likely to prove acceptable for other reasons. 224 NEW YORK STATE MUSEUM The question of shifting the lines is a complicated one and hinges more upon rock conditions, durability, and location of weak zones, than on any possible cost. Advisable changes in lines None of the suggested lines are defensible from a geologic point of view for the reason that a much better one may be obtained by no very serious shifting. In the general consideration of relative advantages of different _ possible locations of the line, it is. believed that the following large features are of most immediate importance: 1 The ridges as opposed to the valleys. 2 The hard formations as opposed to the softer ones. 3 The crossing of few contacts as opposed to crossing many. 4 The location well within a formation as opposed to location aiong a contact zone. It is distinctly preferable from a geologic standpoint (1) to fol- low the ridges, (2) to keep in the hard formations, (3) to avoid many changes from one formation to another, (4) to keep away from contact zones, and (5) to avoid weak zones, if possible, or cross known troublesome zones at the most advantageous point. Recommendations of new lines F, G, H, I The original lines A, B and C are marked on the map in blue [pl. 32]. In addition several trial lines are sketched in yellow, any one of which would give better geological conditions than any of the three original lines. The newly suggested trial lines differ from each other chiefly in the points at which they cross the limestone belts and weak zones. In all of them the central idea has been to follow the gneiss and schist ridges as persistently as possible. All unite at Central Park and are intended to follow Fifth avenue, Broadway, the Bowery and Market street to East river along one of the original lines. North of Central Park they differ from the orig- inal lines. The westerly one crosses the Harlem river at 176th street and may be designated line F. The easterly line may also cross the Harlem river at 176th street and may be designated line G; or it may continue southward and cross the Harlem at 1 55th street. It will then join the first one in the vicinity of 144th street and is called line H. The alternative easterly one which crosses the Har- lem at 155th street and follows Seventh avenue to Central Park is line [. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 225 Details of rock conditions along these lines are as follows: Line F. (Westerly) beginning at Hill View reservowr Feet 7600 Yonkers gneiss — good quality 15 000 Fordham gneiss — good quality 2000 Fordham gneiss — probably 2d grade 1200 Harlem river crossing—partly limestone—3d_ grade 14 800 Manhattan schist — good quality 1600 Manhattanville crossing — 3d grade — some limestone 2600 Manhattan schist—good rock—through Morningside Parle: 800 At south end of Morningside Park — perhaps some lime- stone — 2d grade 1 400 Manhattan schist — good — to junction 12000 Manhattan schist — along Central Park — good 20600 To East river — Manhattan schist —less known’— (fair) (2d grade) 6000 To Brooklyn “ unknown”! 85 600 Lime G Feet 8 400 Yonkers gneiss — good rock 17600 Fordham gneiss — good rock which brings it to the Harlem river where the other line (F) 1s joined. Although the line is about 1400 feet longer, it avoids some low ground (2000 feet) along the east bank of the Harlem river, some of which may be in poor condition. Total length of line, 87,000 feet. Line H Feet 8400 Yonkers gneiss — good quality 23 800 Fordham gneiss — good quality — to Harlem river I 000 Crossing Harlem river — probably fault zone in gneiss Soo Fordham gneiss — good quality 1000 Limestone — 2d grade 1 200 Manhattan schist — good quality — to junction with the first line (F) at 145th street From this point the line is the same as F and G. Its chief ad- vantage is the great distance which it has in Fordham gneiss. Total length of line, 85,600 feet. * Subsequent explorations made by the Board of Water Supply have elimi- nated this unknown ground: See later discussion. 226 NEW YORK STATE MUSEUM Line I Feet 8 400 Yonkers gneiss — good quality 23 800 Fordham gneiss— good quality —to Harlem river 1000 Crossing Harlem river -— probably fault zone in gneiss 4 400 Fordham gneiss — good rock — to 135th street 4600 Inwood limestone — probably fair — 2d grade 2000 Inwood limestone — probably poor quality — 3d grade 1000 Manhattan schist — good quality | At this point the line unites with line F. Total length of line, &2,800 feet. A tabulation of these figures indicating estimated extent of rock types is given below: LINE F LINE G LINE H LINE i Feet Feet Feet Feet ioral lenothy or Immest ena cere oe Oe ee 85 600 87000 85600 83800 Benet in Yonkersveneisse eae ee wee ee 7600 8400 8400 8400 Meneth im Hordham someissen+. see sone ee 17000 17600 25600 29200 Length in Inwood limestone and marginal COMEACES {Sree 6 eRe ee ce ah ee 3600 -3 600, 3400) 8 “6iGon iencth wn Manhattan senistene. seers 51 400 51400 42200 33600 Comparative summary of types of formation (Comparative dis- tances are expressed in percentages) A B Cc F G H I WEOmkerS /ST1EISS 42 so mete ele 7D UOBAS 73. “Oxare EOSOMNOnO gGNe) ordliam! ST1eisse si. penoeee ee eek Sup 5.3 926).3)" 10-6" 20e2 5 2OnOr sane CGontactwones sy: Sea aaa Beaty LOKOM) O43 ihiwood limestone aan... ween AAO). QE) mt Ee) UWS GE EN Miainhiattans SCHISt see eee ue BOu5 "4220. (72S 6020, 950-0) 49.5 ou Ravenswood grano-diorite! ...... 0.0 OL Om 1250.4, OL0) 40053 OL O05 Ono Too little known to classify!..... 7.0 | 2720. 22-06 7.05) Os ps7 Onur 1The Ravenswood granodiorite has been proven by later explorations to extend into the territory here marked as too little known to classify. As a group it is especially noticeable that the new lines F, G, H, I, have a very much lower percentage of contact zones and lime- stone. The percentages of gneisses have been notably increased, and the unknown and questionable formations have been reduced to approximately the lowest terms. GEOLOGY OF THE NEW YORK CITY AQUEDUCT 227 Estimated summary of quality LINE F LINE G LINE H LINE I Feet Feet Feet Feet ood. sock, first. otadex.. os. hi6% 53 400 56 800 54 600 AQ 600 Fair ep SCCONG MAT Lyle see eae oe 23 400 2I 400 22 400 25 200 Poeria: ~hird:. *“ br Heater 2 800 2 800 2 600 3 000 Unknown! (Brooklyn) .......4...: 6 000 6 000 6 000 6 000 85 600 87 000 85 600 83 800 1 All of this rock is now known to be of good quality. In other words these new lines show: LINE F LINE G LINE H LINE I Percent Percent Percent Percent Pet EAE: GOCK © os sess ba fa kona elads 62:3 65.3 63.8 59.1 Second Shao ed at UES A RE AO anes oes Tega ig 24.6 26.1 30.0 First and second grades together....::.... 89.6 89.9 89.9 89.1 MP ECmenAGe LOCKE vs OP iekios waves Sateen es 3.2 220 3.0 3.6 Seerikimauwt ) stron) oN ony. a deco a sale 7.0 6.9 7.0 7a *Results of recent boring explorations show that this ground is first grade also. A comparison on this.basis with the original lines A, B, C indi- cates that these new lines F, G, H, I, make a better showing, especially on first grade rock and that all show decided reduction in the third grade ground. A B Cc F G H I Rigsieorade LOCK. 2.05. 5666 2 bss « 40.4. 40.0). _AG.0: 6253626553, (02281). 50.1 DecOnMeerade TOCK ..c58 660 - Se BEFO.e ALS 10:7 227 03.6 242m 20uh aoc EiteSh tated SECON! 152 ce gee eais cer 8523) (SIO) 165...7). 80.67 | S0.01460-0) 480.1 Mhindvemade rock sof esses es Tet Oe TO) ee ORES OnE. 30 Raker mia vac eee te oes faye ZEON Pat QB | WAKO KONO uae Own re I 1 Now known to be first grade. On geological grounds, therefore, it is confidently believed that any one of the new lines (F, G, H, I) would give decidedly better results than any one of the original ones (A, B, C). The poor and the questionable and the unknown ground can not be wholly avoided by any possible line, no matter how roundabout. In these lines, approximately as drawn, the objectionable points are reduced to a minimum with almost no increase in total length of conduit. The objectionable portions are also restricted in large part to the 8 228 NEW YORK STATE MUSEUM Harlem river, where we already have the experience of the last aqueduct (the New Croton aqueduct) as a guide, and a very few other spots. General conclusions Line I is the shortest possible defensible line. Its chief objec- tonable feature is a rather long stretch, 6600 feet of limestone, from 135th street to Central Park, upon the quality of which there are no data. It crosses the Harlem river fault probably in gneiss. - But it crosses the extension of the Manhattanville fault in lime- stone. Lines F, G and H are almost equally defensible. Line G is longest, but is in some respects — especially in following the ridge crests — one of the best possible locations. It should be appreciated that many other matters, such as municipal works already completed or projected, or matters of engineering practice, are likely to make it necessary to modify any line proposed, and that the final line is more likely to be a com- promise, considering all interests. A graphic representation of the comparative merits of the pro- posed lines is given in plate 33. This is strictly a geologic study. The lines are properly placed on an outline map of the city corre- sponding exactly to those drawn on the geologic map, plate 32. The geologic formations that each would cut are represented on longitudinal sections which follow each line, and the attitude and ‘structure of each formation are indicated. Revised lines Subsequently two revised lines based upon the preceding studies were examined to determine preference. Later one of these, or a slight modification of it, was adopted as the one to be explored. It was soon determined on the same reasoning as was applied to the first group of lines that the most westerly line — the line keep- ing as much as possible within the gneiss and schist ridges — would be the most likely to give satisfactory conditions. By this method of selection the unknown or untested and doubtful ground was reduced to its lowest limits. It was found that nearly all of the very weak spots could be located by inspection in the northern portion of the line, but south of 59th street the question is de- cidedly more difficult because of the heavy drift cover. No rock outcrops occur south of 30th street, and one is reduced to the evidence of deep borings. se) SRE % pe ae ae LEM - POET ST meg heen 1a es ~~ ae “tf = iby ) 7? ; rat RP, 7 : SE sp na es rs i Pa ; i. he ‘vad | . on 4 . » 7 2 < _ - oes ae é 4 ws ’ as ' a N. Y. State Museum Bulletin 146 Plate 33 — y Grariic Geovocic Stupy E . cron SS a ms “ 3 Arternative Lines Inwood Limestone Fordham Gneiss Yonkers Gneiss Ravenswood i l { SOR aii! Grano-diorite pipe) SAN SRE S New York Ciry Ys SS ; g Z = Distaisution Conpuir The attitude of the different forma- “ions and their approximate amounts are indicated by longitudinal sections along the alternative lines whose 4 ance iP courses are indicated in detail on the : cs aa SS SS SSS accompanying geologic map, SSS New York Bay pive® Pian of lines same as on Geologie Mop Original lines -A,B.C,D.E. in blu New lines-F.G,H1. in orange: This limestone can be avoided by running farther South with lines For G before turning to = Wi noe DISTRIBUTION CONDUITS ercioee stcrient ex provost Usts 2000 6 2000F puntg relationship of the 7 folded formations Huoson RIVER Huoson River GEOLOGY OF THE NEW YORK CITY AQUEDUCT 229 Points for exploration north of 59th street It was soon evident that extensive exploratory work would have to be undertaken and the following points were selected at which to begin. : 1 The Harlem river crossing, where the distribution conduit line crosses the river just below High Bridge [see later description]. The only good evidence as to character of rock at this place is from the pressure tunnel of the New Croton aqueduct which crosses the river a short distance above. 2 The Manhattanville cross valley (125th street depression). This is the most important cross depression on the island of Man- hattan. It is apparent after a little investigation that the bed rock floor lies deep and that if it were not for the drift filling the tides would surge through this -valley making a direct connection between the Hudson and East river. It was the least known as to depth and character of any point along the proposed line. 3 The depression between Morningside and Central Park. At that place limestone on the crest of a pitching anticline reaches farther south than on either side and is more deeply eroded. The other zones of large importance are in southern Manhattan the geology of which is a special study. CHAPTER XVIII AREAL AND STRUCTURAL GEOLOGY SOUTH OF 59TH STREET The necessity for exploration in certain sections of this area can not be appreciated without a statement of the local geology and especially of the revision of both areal and structural geology that the writer has based upon an exhaustive study of all the available drill cores and other data to be found in southern Manhattan, East river and Brooklyn. | Below Central Park there is now little geology to be gathered from a study of the present surface. But as far south as 3Ist street the bed rock geology is pretty well known from earlier re- ports and from recent improvements that have exposed the under- lying rock. All of this portion is mapped as Manhattan schist ex- cept one small area of serpentine at 59th street between Ioth and 11th avenues. There is no reason to modify this usage. A careful study of a great number of rock borings from the Pennsylvania Railroad tunnel across Manhattan at 32d street proves beyond question that bed rock is Manhattan schist, including almost all known variations and accompaniments, for the whole width of the island along that line. Still farther southward the points that have yielded exact in- formation about bed rock are less numerous, and below 14th street are confined to deep borings or an occasional very deep excavation for foundations. Even these sources of information are lacking over large areas. The greater number of borings available are along the water front. Their distribution is such as to indicate that the west side and central portion and southerly extremity of the island are all underlain by Manhattan schist. This is true eastward to the East river at 27th street, and as far eastward as Tompkins square at 1oth street and almost to the Manhattan tower of Brook- lyn bridge in that vicinity. To the eastward of these limits, i. e. to the eastward of the line projected from Blackwell’s Island to the Manhattan tower of Brooklyn bridge, there is a more complicated geology. The borings of the East river water front are decidedly variable. They are certainly not all Manhattan schist of the usual types. Those most unlike the Manhattan are at the same time most like some varieties 231 232 NEW YORK STATE MUSEUM of the Fordham, and indicate that these formations both occur. The lack of any data in the beginning of this investigation except on the water front made it impossible to draw more than very gen- eral lines. Drawn in this way, the lines of course are too straight, but it is certain that they indicate more nearly the actual existing areal distribution of formations than any of the maps now in exist- ence.1 They indicate a southward extension of the Blackwell’s Island belt of Fordham gneiss toward the Manhattan tower of Brooklyn bridge. How much of this anticlinal fold of Fordham actually brings this formation to the surface it is impossible to say, but that it may be expected to be encountered along this line is evident. | On the east side a parallel belt of Inwood limestone is indi- cated and this again is succeeded by a Fordham gneiss area which occupies the rest of the eastern margin. Explorations made along the line of the gas tunnel across East river at 72d street? indicates comparatively narrow belts of limestone there in both the east and west channels. The limited width of limestone at these points, together with the occurrence of two strongly de- veloped disintegration zones, seem to indicate rather extensive squeezing out and faulting of this formation along fault planes 17In the summer of 1908 the writer was assigned the task of studying in detail the evidences of geologic structure beneath the drift in southern Manhattan. Before any drilling was attempted in the city by the Board of Water Supply, a thorough canvass was made of all previous borings in this district and the cores and records were personally inspected. More than 300 such borings were found in which some of the core could be secured for identification and classification as to formation and condition. Most borings were given no weight at all in the final summary of this evidence unless the rock core or at least fragments of it could be secured. After all of these newly assembled data were tabulated and plotted on the map, it was evident that if the identifications were correct the areal and structural map of southern Manhattan needed extensive revision. A new map therefore was made and presented to the chief engineer of the Board, October 30, 1908. This has been used since as the basis for exploration of the Lower East Side section. This original tabulation and map only slightly modified was published under the Areal and Structural Geology of Southern Manhattan Island [N. Y. Acad. Sci. Annals, April 1910, v. I9, no. II, pt 2]. The extensive explorations of the board have made further revision necessary [see accompanying map, pl. 34]. Exploratory boring is still in progress (October 1910) and some slight modifications of boundary lines may yet be made. 2 This is taken from Prof. J. F. Kemp’s description of The Geologic Sec- tion of the East River at Seventieth Street, New York [N. Y. Acad. Sci. Trans. 1895. 14:273-76]. ; eels 5 ey > Leg. Y FEZ : > MRL Z i © Ree aes eget ee oe ERE» yf oy s\) y 7 A “: Gy, @ Wy, Mi 46 m2 SS way >: Base map reproduced from a copyrighted map by B. Belcher Hyde, 5 Beekman street, and here used by permission N. Y. State Museum Bulletin ; aeuaee Lt No reurrcs, i 46 2 eo > = = ? >0 wet bas wt Ss 3s ZzEs ae ze Sing SE Q Eos zs os 52 a= Os } 222 O® Ses jt" Ps Zz fw 8 os a ose? ae o 3 we £08 ox ira) epee ZE == uso8 Vi wes NE 52 ageae we © 1°38), | = = = : 2230 Gus LJ Zs KS as 3 WS fe Yeates =i ef <° o> 15 fl Y=" s, xES xr? >. aD Dos 1\-“S: wl oi fa” psu] als 5 his QS -200 | Ay zy y i He n il Col tecg Ne H ® SN | ed aS ; Re Bes | | | id (ees i PRRs ai -300 iv | 8 RR By BS OMA ow GH HS GSR IMENT RR, SU —400 Manhattan i iB S$ Inwood Dail See is He wf Ns iol # ie -400 / | as cy 7 Te + hla de a oi bye OO Schist | aN Limestone & “ah ld oF v ll. nN Aral Hil i | x — 400 H aes S HH SiH ‘ Hy & in 9 i 2 ; i ‘ fy - 500 3 : A ae aT i ak i —600 Inuroed Limestone I! d i i ql Se os 6 ft 2 HI i 3 “fl Fordham Gnevss Serves -600 LH = 2 P ii A mostly granodiorite 700 Fordham Gneiss Serves [' I: i z ou sll i I i -700 fi with oecasiona/ ‘haa = a Ve limestone be wy i — 800 BS bed ) Fordham Gneiss Series with many narrow Interbedded Limestones we -GOO — 900 -900 City of New York -/000 000 BOARD OF WATER SUPPLY -//00 400) CATSKILL AQUEDU CT Shisp= S = GEOLOGIC DETAIL OF LOWER EAST SIDE : } fF < QYfE= Deore): Pp oftle line 1's intended to Ma ZS. = N Lippe are prosected parallel lo Sike mark the fim) -ock decay as interpreted = y W; hole*Lé ald (Ole 3 Vane iemg?! of rock aecay age Kecovery OVEl 25 fe Shown this Goronmate bearirg of strike 1s NLEL 200 from borings Each proms ment depiess/oi Kecovery Under , 2» 9 | Y) 200 0 eet F OCTOBER 18, 1910 probably tncheates a cresh 2078 belonging No fecovery a7) ry) i to a fault. | j CHAPTER XX THE GENERAL QUESTION OF POSTGLACIAL FAULTING WITH ITS BEARING ON THE PERMANENCE OF ENGINEERING STRUC- TURES. Evidences of postglacial faulting and other recent movements have of late attracted a good deal of attention. The experience of San Francisco in the exceptionally disastrous earthquake and fire, traceable directly to earth movements of the nature of faulting which dislocated or injured the water conduits rendering them use- less, is fresh in the minds of men everywhere who have public responsibilities of this kind. If displacements are occurring at the present time, or if any related movements are continuing, or if there is evidence of recent disturbances of this sort in this region, they have a decidedly important bearing upon the permanence of all engineering structures that cross them. No undertaking is more vitally concerned with this question than the Catskill aqueduct. Although the principal factors to be taken into account have been considered in other connections. [see “Faults”? and “ Folds,’ pt 1] a unified statement may encourage a more intelligent understanding of the bearing of these structures in southeastern New York on this specific question. The region included in this discussion extends from the Catskill mountains to New York city. It will be convenient, for the pur- poses of this argument, to divide the whole area into three districts whose boundaries are determined by decided differences in com- plexity of geologic history. These lines necessarily follow closely the boundaries of greater stratigraphic unconformities. The youngest groups of strata have suffered only such changes as have accompanied movements of later geologic periods. But before they were formed the underlying groups of rocks were just as pro- founaly affected by earlier disturbances. In this region, at least, three such groups of large importance exist. The oldest or lowest has been affected by riot only everything that has influenced the younger strata but by disturbances of a still earlier time which very much increase their complexity. On this basis it is convenient to think of the three districts as follows: A Catskill district. Including that portion of the region west and northwest of the Shawangunk mountains and marked by the 271 is) os) 7 NEW YORK STATE MUSEUM prevalence of Siluric and Devonic strata, i. e. all strata above the Kudson River slates. These strata have been affected by only one great mountain-making movement — that of the Appalachian fold- ing, and minor disturbances of still later date. B Hudson river district. This includes that portion of the region lying between the northern border of the Highlands and the hawangunk mountains. It is marked by the prevalence of Cam- ric and Ordovicic strata, i. e. Hudson River slates, associated with ‘appinger limestone and Poughquag quartzite as the chief bed rock. These strata have been affected not only by the Appalachian folding but also by a still earlier one — that of the Green mountains and the Taconic range. They were folded mto mountain ranges and worn down in part again before the Siluric and Devonic strata oi district 4 were im existence. Therefore as a structural problem this district (B) is approximately twice as complex as the other. C Highlands district. This includes all of the region com- monly known as the Highlands of the Hudson as well as the rest of the area south of the Highlands proper to New York city. Its rocks are the oldest —- much the oldest. They had been folded into mountain structures and in part worn down before any of the others were accumulated. They have also suffered extensive igneous intrusion so that im places these igneous types prevail. And besides they have been metamorphosed far beyond the pomt of any other group. No other series of strata has been so pro- foundly affected. They form the lowest group. All thimgs con- sidered this district should be structurally three times as compli- cated at the first one (4), and adding the igneous and metamorphic complexities, it is probably more near the truth to consider this Highland district’ four or five times more complex. All of the formations from-the oldest to the Middle Devonic are involved. For the specific formations and their succession and rela- tion the reader is referred to that discussion in part 1 [see p. 29, et. seq.|- |p if) = Structural features Except the most westerly part of the region, that occupied by the Upper Devonic strata, all formations are compressed into iolds. Many of the smaller folds, especially those in the Catskill district, are still complete. The easy subdivision of strata possible in this district also simplifies the problem of detecting small changes of altitude. But for the most part the larger folds have been beveled =,0f extensively by surface erosion so that only the truncated limbs GEOLOGY OF THE NEW YORK CITY AQUEDUCT 273 are now to be seen, and the strata therefore appear as narrow belts that dip steeply into the ground. This is more marked in the Hudson river district than in the Catskill, and 1s still more strikingly true of the Highlands. There are evidently at least three different epochs of folding inter- rupting the processes of sedimentation and followed by periods of erosion before sedimentation was again resumed. These breaks constitute so called stratigraphic unconformities and occupy the relative positions indicated in the foregoing tabulated scheme [see ptr). In each epoch of folding the compressive forces accomplishing this work. seem to have acted in a southeast-northwest direction causing successive series of folds with a northeast-southwest trend. The total amount of crustal shortening accompanying these move- ments is not known, but that it must be many miles is indicated by the fact that the strata of the older series of formations stand pre- vailingly on edge. All stages between small amount of movement to very great displacement are represented. Accompanying the folding in each epoch there has been a ten- dency to rupture and displacement of the “fault” type. There are multitudes of them varying from movements of too little amount to be regarded in a broad way to those of several hundred feet. Most of the larger and more persistent ones are strike faults and follow. the main ridges or valleys, sometimes governing the location of escarpments or gorges. Dip faults crossing the formations also occur and doubtless have guided the adjustments of many tributary streams, and occasionally portions of the larger water courses. The thrust fault is most common. This is especially true of the larger ones and particularly those parallel to the trend of the other struc- tural features. The chief effects of these movements may be summarized as follows: 1 Formations are cut out of their normal order and nonadjacent ones are brought in contact. 2 Cliffs (escarpments) and sharp gulches are more common. 3 Crush zones (belts of brecciated material) are developed. 4 The crush zones give an additional control of stream adjust- ments. All of these effects are common. Many of those faults dating back to the earlier epochs are obscure and not readily located. Many of the older weaknesses of this sort have been healed by recrystalli- 274 NEW YORK STATE MUSEUM zation so that they are now as sound as any other portion of the rock. A good deal depends upon the type of rock and the conditions under which the movement took place. In some of the more open ones, circulating water has seriously affected the rock and in places there 1s extensive decay even in the harder crystalline formations. Age of the faulting. The chief epochs of folding and faulting are those of the mountain-making movements — one Precambric, another Postordovicic, and still another Postcarbonic. All of these date very far back in geologic history, and since the last of these, othing akin to them in importance has been felt in the region. In Posttriassic times however there was small faulting south of the Highlands, that affected the areas of Triassic rocks of New Jersey and Connecticut. Whether or not there continued to be slight movement along some of the older lines it is now impossible to say. It is at least clear that all of the great movements belong to very ancient time, and that the last period of geologic time as we know it for this region, has been one of comparative stability. The chief exception is evidently con- nected with the continental elevations and depressions of the glacial epoch. Recent movements. The effects of glaciation make it possible to determine whether or not there has been further movement in postglacial time. Conditions are not everywhere favorable enough to detect minute changes, but where they do obtain, the evidence is capable of very definite interpretation. The essential features of these conditions are 1 A bed rock ledge that has been left well smoothed by glacial scouring. 2 Protection from postglacial destruction so that the original unevenness as left by the glacial smoothing can not be mistaken. If on such a ledge, as now exposed, there are steplike offsets or minute escarpments that could not have remained had they been present during the ice action, then there must have been displace- ment to this extent, since the original smoothing took place. A few such evidences have been found in New York and New England, and have been noted in geologic reports. W. W. Mather in his report on the First District of New York (1843) pages 156-57, was the first. The data as now known may be found in the last bulletin of Geologic Papers of the New York State Survey [see N. Y. State Mus. Bul. 107 (1907) p. 5-28]. The following para- GEOLOGY OF THE NEW YORK ‘CITY AQUEDUCT 275 graphs are intended as a brief summary and comment on the facts as there given: | Localities where some postglacial displacement has been detected. 1 Copake, N. Y., on the eastern border of the State near the southwest corner of Massachusetts 2 Rensselaer, N. Y. Sy oouth, lino, Nai. 4 Defreestville, N. Y. (near Troy) 5 Pumpkin Hollow, N. Y. (near Copake) 6 Kilburn Crag, N. H. fF Port Kent N: ¥> (incerta) 8 Attleboro, Mass. In addition to these there is reference to similar occurrences at St John, N. B. and in the province of Quebec. All of the known localities lie a considerable distance beyond, north and northeast, of the Catskill aqueduct line. Causes of displacement. In southern New York all of the cases of postglacial faulting yet discovered lie in the area of slates belonging to the Hudson River series. Whether the belt now occu- pied by this formation is therefore to be considered the most un- stable zone, or whether there is some tendency to slight readjust- ment inherent in the slates themselves causing these movements, is not clear. It would seem consistent with known recent geologic history to connect these displacements with the general elevation and subsidences accompanying and following the glacial occupation. It is perfectly clear that the whole continental border in this region suffered considerable subsidence during glacial time. Also the ter- races and deposits along the Hudson prove beyond question that during the ice retreat, at the very close of the glacial occupation, the land surface stood from 80 to 150 feet lower than now. There- fore an elevation of this amount has occurred in postglacial time, and probably, judging from the condition of the terraces themselves, took place soon after the glacial ice withdrew. The stresses and inevitable warpings accompanying these mass movements seem to be sufficient to account for all displacements known to be of this age. There is nothing in them that necessarily promises a renewal of mountain folding. But it appears that the movements have almost all been of the thrust character and in this respect they differ not at all from the commoner type of the region. 276 NEW YORK STATE MUSEUM Amount of displacement. he greatest throw noted on any single Postglacial fault in eastern New York is given by Wood- worth as 6 inches, and he remarks that this 1s imperfectly shown. Usually the displacement is distributed over a zone in which several small faults occur instead of a single larger one. This may mean that the whole disturbance is essentially superficial. At South Troy it is stated that a total displacement of 12 inches is thus distributed through a number of small fauits within a dis- tance of 30 feet. At Rensselaer a total of 5 inches is given. At Defreestville a total of 13 inches is indicated in a distance Of Teeverec: At Copake, at two different spots, a total of more than 7 ches was measured within a space of 12 feet. Woodworth thinks that the total displacement for the locality may exceed 2 feet. At Pumpkin Hollow a total of 17 inches is estimated. Conclusion. If such rates prevail over larger areas beneath the drift, it is clear that rather profound changes would be indi- cated. But thus far there is no indication of such continuity. Likewise if it were certain that the movements are now in progress, it would be a matter of greater concern. But there is no direct evidence to prove it. | Estimates of the length of postglacial time differ greatly. The shortest ones worthy of consideration range from about 5000 to 10,000; the longest run above 100,000 years. Some intermediate value is probably nearer the truth — say 25,000 years. Adjusting the postglacial faulting problem then to these time estimates the summary of it all would be as follows: Somewhere within postglacial time, i. e. approximately 25,000 years, move- ments of strata have developed at a few places in eastern New York that appear as small faults with total throw in each locality varying from a few inches to perhaps as much as 2 feet. Whether the movement has been gradual and continuous or concentrated largely into some small portion of this time is not known. Whether the effects are extensive or, on the contrary, very local and super- ficial, is likewise unknown. But in any case there are no known instances of violent and large displacements, such as would be likely to cause great damage to sound structures, in this region in postglacial time. LED EX Appalachian mountain-folding, 66, 73. Aqueduct, see Catskill aqueduct. Arden point, 97, 104. Arden point line, 85. Artesian flows, 142. Ashokan dam, construction of, 13; elevation of reservoir, I7; stone used in construction, 38; geologi- cal features involved in selection of site for, 109-16; location map, 113; Olive Bridge preferable location, 116; to be finished first, 183. \spidocrinus scutelliformis, 42. Athyris spiriferoides, 38. Atrypa reticularis, 40, 43. spinosa, 40. Atwood, T. C., acknowledgments to, 7; division engineer, 237. 63, Beaver Kill, 110. Becraft limestone, 42, 55, 126. Bensel, John A., member of Board of Water Supply, 13. Berkey, Charles P., consulting geolo- gist, 6, 19, 75; cited, 48. Binnewater sandstone, 44, 55, 133, 134, 140; porosity, 135. Bluestone, character and _ quality, 117-23; economic features, I10; petrography, I19Q—23. Borings on the lower east side, tabu- lations and interpretations, 254-65. Breakneck ridge, 85, 91-95, 100, 163; quality and condition of rock, 106- a Brink, Lawrence C., acknowledg- ments to, 6; division engineer, 21, 149, ISI. Bronx valley, geologic cross section, 193. Brown, Thomas C., Esopus division, 125; on limestone rocks, 140. 126, employed on observaticn o-- ae Brush, William W., acknowledg- ments to, 6; division engineer, 14, Ba OTS: Bryn Mawr, geologic section at, 205; comparison with shaft 13, 212. Bryn Mawr siphon, 201-8. Bull mountain, 163. Calyx drill, 26. Cambric quartzite, 102. Cambro-Ordovicic formations, 45-46, 50; 108: Carson, J. -P*-cited)-200: Cat Hill gneissoid granite, 52, 57. Catskill aqueduct, water supply pro- ject, 90-16; generalities of construc- tion, 14-15; estimation of cost, 15; present plans for, 15; time for completion, 15; problems en- countered in the project, 17-24; gathering data, 21-23; relative val- ues of different sources of infor- mation and stages of development, 25-28; geologic problems, 75-276; general position of aqueduct line, 77-80; location map, 8o. Catskill creek, IT. Catskill district, general geology, 2 74; of simple structure, 31; post- glacial faulting, 271-72. Catskill. formation, 47% 55, 63. Catskill Monadnock group, 73. Catskill supply, area in square miles, 11; daily supply in gallons, 11; estimated daily supply, 11; esti- mated cost, II; storage in gallons, II; part of supply available by TOTS. BS. Catskill system, parts of, II-14; con- struction of certain parts in ad- vance of the rest, 13. Catskill watersheds and aqueduct, ATG TA Caves, 137. Cedar Cliff, 103. Cement beds, 44. Cenozoic time, 64. Chadwick, Charles N., member of Board of Water Supply, 13. Chonetes coronatus, 38. mucronatus, 38. Chop drill, 26. Clapp, Sidney, 109. Clark, cited, 44. Clays, III. Coastal plain, 73. Cobleskill beds, 44, 55, 126. Coeymans limestone, 43, 55, 126, 133. Cold Spring, 85, 163. Conglomerates, better quality of wall than limestones, 140. Continental elevation, 67-60. Cortlandt series of gabbro-diorites, assistant engineer, cre ee 52, 53, 5/- Coxing kill, 127, 128. Coxing kill section, 135-36; struc- tural geologic detail, 136. Cretaceous deposits, 36-37, 54. Cretaceous peneplain, 67. Cronomer hill, 154. Crosby, W. O., consulting geologist, 6, 19, 75; cited, 36. Cross sections, Rondout valley, 140. Croton aqueduct, study oi shait 13 and vicinity, 200-14; comparison of Bryn Mawr and shait 13, 212- 14; map showing location, 239. Croton lake crossing, 183-89. Croton river, average daily fiow, 9. Croton water, average daily consump- tion, 9. Crows Nest, 100, 163. Crystallines, south of the Highlands, 47, 50; older, 57- Dalmanella testudinaria, 46. Dalmanites selenurus, 40. Dana, J. D., cited, 48; mentioned, 46. Danskammer crossing, 85, 97, 103. Darton, mentioned, 46. Davis, Carlton E., acknowledgments to, 6; department engineer, 13. 78 NEW YORK STATE MUSEUM Davis, J. L., tests of Kensico rocks, 199. Delancey and Clinton street section, structural geology, 253-66. Delivery conduits, geological condi- tions affecting the location of con- duits, 215-29. Devonic strata, 37-43, 55- Diabase, 37, 240. Diamond drill, 26. Dikes, 106; pegmatite, 52. Dinnan quarry, 198. Division engineers, responsibility oi, = Driit, kinds of, 33-36; glacial, 32-36, © 54, 100, 202. Dwight, mentioned, 46. East river crossing, 233, 238. East river section, 250-53; structure, 233- Engineers, division, responsibility oi, =a fh Esopus creek, 11, 69, 77, 112, 128. Esopus division of Northern Aque- duct Department, 125. Esopus shale, 40, 55, 126, 140; thick- ness, 133. | Esopus valley, geologic cross section, 78. Esopus P45, Exploration zones, special, 237-70. watershed, development of, Fault zones, 206. Faults, 60-62, 135, 163; postglacial, general question of, 271-76. Favosites helderbergia, 43. Ferris quarry, 198. Firth Cliffe, 153. Flinn, Alfred D., acknowledgments to, 6; department engineer, 13, 215. Folds, 59-60, 272. Fordham gneiss, 47, 52, 57, 62, 185, IQI, 192, 202, 206, 217, 218, 219, 220, 221, 225, 220,, 232, 233, 234, 237, 238, 255, 257, 258, 260, 261, 262, 264, 265, 266, 268. INDEX TO GEOLOGY OF THE NEW YORK CITY AQUEDUCT 274 Formations, summary of, 54-57. Foundry brook, 27; rock condition at, 163-60. Foundry brook valley, structural de- taude TOS. Garden quarry, 198, 199. Geographic features, 30-31. Geographic history, 65-74. Geologic conditions affecting the Hudson river crossing, 97-107. Geologic knowledge, practical appli- cation to engineering plans, 19. Geologic problems of the aqueduct, 75-276. . Geology of region, 29-74; summary of formations, 54-57; outline of history, 62-65; local summary, 2605— 66. : | Glacial drift, 32-36, 54, 100, 202. Glacial period, 64, 71. Gneisses, 176; dioritic, 198, 199; Grenville series, 50-52, 57. See also Highland gneiss. Grabau, A. W., cited, 37, 44. Granites, 99, I00, 100; gneissoid, 198; of the new Ferris quarry, 108. Grassy Sprain valley, 203. Gravel, IIo. Gravel hillocks, 110. Gravel streaks, I1I-12. Grenville series, 50-52, 57, 62. Hamilton shales, 38, 55, 78, 119, 126, 140. Harbor hill moraine, 35. Harlem river crossing, 237, 238-44; map showing plan of exploratory borings, 239. Hartnagel, cited, 44; mentioned, 154. Healey, John R., acknowledgments to, 6; exploratory work by, 237. Henry street, interpretation of hole No. 207 on, 261-65. Hester street, interpretation of hole No. 202 on, 259-61. High Falls, 125, 127, 133. High Falls shale, 44, 55, 126, 133, 134. 135; porosity, 135. Highlands, 30-31, 73, 81; crystal- lines south of, 47, 56; postglacial faulting, 272. Highlands gneiss, 50, 57, 99, 102, 154, 163. Sce also Fordham gneiss. Highlands group, crossings, 97, 103- 4, 105; more defensible as a route for the aqueduct line, 103. Hill View reservoir, 215; elevation, V7. Hipparionyx proximus, 41. Hobbs, mentioned, 95. Hogan, > Thomas! Ey vision engineer, I25. Hornblendic gneiss, 263. Hudson river, 60; water to be used for fire protection, 10; wash bor- ings, 26; depth of buried channel, 89; submarine channel, 90-01; Storm King-Breakneck mountain profile, 91-95; origin of the present course, 95-96; crossing, geological conditions affecting, 97-107; out- line map showing possible cross- ings, 98; difference of structure in crossings, 104; postglacial fault- ing of district, 272. Hudson river canyon, 81-96; points of exploration, 83-88; comparative sections at Peggs point and Storm King, 92; study of profile, 94. Hudson River slates, 46, 56, 83, 100, 102; 103, :120,, 135,137, E40, emer WS Suen 27. Hudson schist, 201. Hurley, 127. assistant di- Idlewild, 154. Igneous types, 52-54. Imperviousness and insolubility, 13&- 39. Inwood limestone, 47, 49-50, 56, 172, 185, 191, 192, 201, 202; 210; 21a 217; 218, (210, -220; 227) 226. aan 237, 238, 240, 242, 243, 245, 246, ZAG. (254) SEGe 250. 201, 202. aoe. 268, 269. 280 Ithaca beds, 38, 55. Jameco gravels, 39. Jerome Park reservoir, interbedded development of limestones in vicin- ity of, 268. Jura-Trias formations, 37, 54. Kemp, James F., acknowledgments to, 6; consulting geologist, 6, 19, 75 3 Cited) ele. 232: Kensico dam site, geology of, I9I- 94. Kensico quarries, stone of, 195-200; additional tests, 190. Kensico reservoir, to be enlarged, 132 Kripplebush, 127. Kripplebush section, 129-31. Laminated sand and clay, III. Laminated till, IIo. Langthorn, J. S., acknowledgments to, 7; division engineer, 2I, 109. Leperditia alta, 44. Leptaena rhomboidalis, 40, 42. Leptocoelia acutiplicata, 40. Leptostrophia magnifica, 41. perplana, 40. Libertyville, 149, 150. Limestones, 99, 100, 176; resistance to solution, 139; analysis of, 139; of Sprout Brook valley, 171; in- terbedded, older than the Inwood, 266-70. Liorhynchus mysia, 38. Little Stony point, 85, 97, 104. Location map, 80. Long Island, Cretaceous and Ter- tiary strata, 32; glacial deposits, 35-36. Lower East Side zone, 238. Lowerre quartzite, 47, 50, 56. McCarthy, C. H., boring equipment owned and operated by, 141. Manhattan schist, 47, 48-49, 56, 171, Teas. TOO) MGOl, MOS) ZOl. eigeeeno: NEW YORK STATE ——— MUSEUM 219, 220,,, 221, 1225, .220, 233, 235 237, 238, 240, 241, 242, 243, 244, 245, 246, 247, 248, 240, 254, 257, 261, 265, 268, 2609. Manhattanville cross valley, 237, 244- 45. Manlius limestone, 43-44, 55, 126, 133, 124. Marcellus shales, 38, 55, 126. Matawan beds, 37, 54. Mather, W. W., cited, 268, 274. Merrill, cited, 48. Merriman, Thaddeus, acknowledg- ments to, 6; assistant chief engi- MEET, is) TOG, Mesozoic time, 64. Miocene deposits, 36. Miocene fluffy sand, 54. Moodna creek, 103-4; wash borings, 265 (course Of155—50: Moodna valley, ancient, 153-02; sta- tistics, 160. Morningside to Central Park sec- tion, 245-50. Mountain-forming 60. movements, 59- New Ferris quarry, granite, 108. New Hamburg, 81. New Hamburg group, crossings, 97, 102—3, 105. New Hamburg line, 83-85. New Paltz, 140. ew Scotland shaly limestone, 42, lope UAL oe New York-Wesichester district, 30. New York city, gorge at, 91; sec- tions of gorge at 32d street, 92; geological conditions affecting the location of delivery conduits, 215- 29; areal and structural geology south of soth street, 231-36; struc- tural geology of the lower East side, 253-60. Newark series, 37, 54. Newburgh, 154. Northern aqueduct first, 183. 2 to be finished INDEX TO GEOLOGY OF THE NEW YORK CITY AQUEDUCT 281 Oil-well rig, 26. Olive Bridge, 110; site, 112-14; pref- erable location for the proposed Ashokan dam, I16. Oneonta formation, 38, 55, I19. Onondaga limestone, 39-40, 55, 78, T20, 127, 120. Oriskany beds, 40, 55, 120. Orthothetes woolworthanus, 42. Pagenstechers gorge, 154, 155, 159. Paleozoic time, 63. Palisade diabase, 37, 54. Pebble beds, 111-12. Peekskill creek, 172: Peekskill creek valley, structure of, 175-82; geologic cross section and detail of borings, 180. Peekskill granite, 52, 53, 57. Peggs point, borings, 89; gorge at, QI, 92. Peggs point, crossing, 83, 97, 103. Pegmatite, 53, 57, 185; dikes, 52. Peneplain, Cretaceous, 67. Pennsylvania borings opposite 33d street, New York city, 80. Phyllite, 175-76, 181. Physiography, 30-31, 65-74. Piedmont belt, 73. Platyceras dumosum, 40. nodosum, 4I. Pleistocene glaciation, 71. Pliocene deposits, 36, 54. Pompey’s cave, 137-38. Porosity tests, 142-47. Porosity of Kensico rocks, 199. Port Ewen beds, 40, 42, 55, 120. Postglacial faulting, general ques- tion of, 271-70: Poughquag quartzite, 47, 56, 100, 172, £70, Tote72) Pressure tests, 27. Pumping experiments, 142-47. Quartz, 202. Quartzite beds, 90, 100, 176. Quaternary deposits, 32-36, 54. Raritan formation, 37, 54. Ravenswood granodiorite, 52, 53, Big 2204 220.) 220° 233." B52 260. Rhipidomella oblata, 42. Ridgway, Robert, acknowledgments to, 6; department engineer, 13. Rondout cement, 44. Rondout creek, 11, 69. Rondout creek section, 131-35. Rondout siphon statistics, 141-42. Rondout valley section, 125-47; en- gineering problems, 17-19; geology, 31; special features, 137-40; analy- sis of limestones, 139; cross sec- tions, I40. Ronkonkoma moraine, 35. Rosendale cement, 44, 45. Rosendale limestone, 126. 57; 205, St Nicholas Park, 246. Sanborn, James F., acknowledg- ments to, 6; division engineer, 21, 125, TAO; Sands 110} sii Sandstones, 100. Saw Mill valley, 200. Schistose beds, 99. Schoharie creek, II. Schoharie shale, 40, 55. Sedimentation structures, 58. Shales, better quality of wall than limestones, 140. Shaw, Charles A., member of Board of Water Supply, 13. Shawangunk conglomerate, 45, 55, 627-126, SIZ 7) 143) 43h i364 140r thickness, 136; overthrust, 137. Shawangunk mountains, 31, 127. Sherburne beds, 38, 55, 100, 119. Shot drill, 26. Sieberella galeata, 43; figures, 43. pseudogaleata, 42; figures, 42. Siluric. Stkatay 49-4550 55: Sing Sing marble, 201. Siphon line, total borings on, 14t. Skunnemunk mountain, 153, 154. to CO bo Smith, J. Waldo, credit due, 5; chief engineer, 13. Smith, Merritt H., acknowledgments to, 6; deputy chief engineer, 13; department engineer, 14, 183. Smith, Wilson F., acknowledgments to, 7; division engineer, 21, I9QI. Snake hill, 153. Solubility, question of, 138. Southern aqueduct, general location map, 184; terminus, 215. Southern aqueduct department, 183. Spear, Walter E., acknowledgments to, 6; department engineer, 14, 215. Special exploration zones, 237-70. Spencer, J. W., cited, 9o. Spirifer arenosus, 41; figures, 4r. concinnus, 42. macropleura, 42; figures, 43. mucronatus, 38; figures, 39. murchisoni, 41. perlamellosus, 42. Sprague & Henwood, boring equip- ment owned and operated by, I4I. Sprain brook, 203. Springtown, 149, 150. Sproul, A. A., acknowledgments . to, 6; division engineer, 21, 172, 175. Sprout brook, 175, 177; geology, 17I- 74; geologic cross section, 173. Staten Island, Cretaceous and Ter- tiary strata, 32. Stockbridge dolomite, 201, 212. Stony Point, 177. Storm King crossing, 85, 9I-95, 97, 104, 105; trial profile, 94. Storm King gorge, 89, 92, 156. Storm King granite, 52, 57, 100, 104; quality and condition of rock, 106-7. Storm King mountain, fault along the southeast face of, 163. Stratigraphy, 31-57. Strophalosia truncata, 38. Stropheodonta becki, 42. Strophonella headleyana, 42. Strophostylus expansus, 4I. Structural features, 58-62. Styliolina fissurella, 38. NEW YORK STATE MUSEUM Surface configuration, history of, 66. Swift, William E., acknowledgments to, 6; division engineer, 21, 83, 163. Taonurus caudagalli, 4o. Tertiary deposits, 36-37, 54. Tertiary incomplete peneplanation, 69-70. Tertiary reelevation, 70-71. Thirlmere aqueduct of the Man- chester, England, Waterworks, 138. Thirlmere limestone, average of five analyses, 139. Tibbit brook valley, 203. Till, 110. Tompkins Cove, 177. Tongore site, 114-16; plan and geo- logic section, 114; detail of drift character, II5. Topographic features, 30-31. Tuckahoe marble, 2or. Tuff crossing, 83. Uncinulus campbellanus, 42. Unconformities, 58-59. Valhalla, ror. Van Ingen, cited, 44. Veatch, cited, 35, 36. Wallkill river, 60, 128. Wallkill valley section, 149-51; drift conditions, 25. Wallkill-Newburgh district, 31. Wappinger limestone, 46, 56, 83, 100, 102, 354. 172, 270,. Tole 2c Wash rig, 25, 81. Water, increase in consumption, 9; reports on available sources of supply, 10. See also Catskill sup- ply. Water Supply Board, staff, acknowl- edgments to, 7; members, 13; de- partments, 13-I4. Wegman, cited, 209. West Hurley, 77, 78. INDEX TO GEOLOGY OF THE NEW YORK CITY AQUEDUCT 283 West Point location, 104. Woodlawn, cited, 209. West Shokan, III. Woodworth, mentioned, 276. White, Lazarus, acknowledgments to, 6; division engineer, 21, 125, | Yonkers gneiss, 191, 196, 197, 198, 142. 202.257. BIG 210, 220, 221. 2a Wilbur limestone, 44. 226; of superior durability, 200. Winsor, Frank E., acknowledgments to, 6; department engineer, 14, 183. | Zaphrentis prolifica, 40. We oy : i i at Dy I ty That, an De ain) aL oh ee i) ie Verve Pe AD v4, van eal a, q f na - i) ikea one ey , a nay A in} ee 7 ol = ‘i 7 a n aa , ie ae a8 on on . a 7 ih, i} PPM as ua Pot iy ad or ues, a : te i= ribs = . 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