Annual report of the Regents - New York State Museum.

. SS Be.
SAMHSA VAAN
S

~ . Ss
S SS :
“ ~ S\

SASS

FOR THESPEOPEE

FOR EDVCATION |
FOR SCIENCE

LIBRARY
OF

THE AMERICAN MUSEUM
OF

NATURAL HISTORY

University of the State of New York.

NEW YORK STATE MUSEUM

FORTYONINTH ANNUAL REPORT

OF THE

reek NTS

1895

WOE. 2

REPORT OF STATE GEOLOGIST AND FIELD ASSISTANTS

ALBANY
UNIVERSITY OF THE STATE OF NEW YORK
1898

x

for

~

16.

17.

CONTENTS.

Title,

Contents,

Report of the State Geologist,

The Stratigraphic and Faunal Relations of the Oneonta Sandstones and Shales, the Ithaca

and Portage Groups in Central New York; by JoHN M. CLARKE, . 5 5 : 5

The Classification and Distribution of the Hamilton and Chemung Series of Central and

Eastern New York, Part 1; by CHARLES S. PROSSER, 4 3 °
The Stratigraphic Position of the Portage Sandstones in the Naples valley and the Adjoin-
ing Region; by D. Dana LuTHER,
The Economic Geology of Onondaga county, New York; by D. Dana LuTHER, . A 5
The Structural and Economic Geology of Erie county; by Irvine P. BisHop,
Geology of Orange county; by HEINRICH Rims, 3 : ; : . : 5 : -
Report on the Crystalline Rocks of St. Lawrence county ; by CHARLES H. SMyrTH, JR.,
Report on the Geology of Clinton county; by Henry P. CUSHING,
Preliminary Report on the Geology of Essex county; by JAMES F. Kemp, . .

Sections and Thickness of the Lower Silurian Formations on West Canada creek and in
the Mohawk valley; by CHARLES S. PROssER and EpGaR R. CUMINGS, : :
Report on the Tale Industry of St. Lawrence county; by CHARLES H. SMyTH, JR., . :
Physical Tests of the Devonian Shales of New York State to Detérmine their Value for

the Manufacture of Clay Products; by HEINRICH RIEs,
The Discovery of a Sessile Conularia; by R. RUEDEMANN, . : 5

Notes on Some Crustaceans from the Chemung Group of New York; by JOHN M. CLARKE,
5

PAGE.

27

83

699

REPORT.

Orrick oF THE STATE Gronoaist, Room 32, Srare Hatt, }
ABany, N. Y., April 24th, 1896. {
To His Excellency Levi P. Morron, Governor of the State of New York:
Str :—I have the honor to submit the annual report of the State
Geologist, embracing an account of the work done in the field and office.

The geologic map of the State, to which reference was made in my
report of last year, has been completed so far as we had information in
regard to the distribution of the several formations at the date of its sub-
mission, This map has been printed in colors under the direction of the
United States Geological Survey in Washington, and 400 copies have been
presented to the State of New York for distribution to educational insti-
tutions and departments, as well as to the members of the Legislature. The
distribution of these copies has been essentially completed.

The field work of last season was carried on with special reference to

~ completing the map in such portions of the State as were yet incompletely

surveyed, and this work has contributed to our knowledge of the distribu-
tion and accurate limits of the geologic formations in the several counties
under survey. The knowledge thus acquired will enable us to add much
new matter to the map, and to reduce the uncolored areas in any future
edition. At the same time attention has been given to the economic resources
of such portions of country as have been examined, and the result will appear

under the head of the counties described in the report.

The same method of work as heretofore mentioned has been continued,
and the services of the professors in several of the colleges have been secured
during their vacation time, the State incurring only their traveling and field

expenses,

Professor Charles 8. Prosser of Union College, has been engaged in the
central portion of the State, and Professor Clarke, assistant State geologist,
has been giving special attention to the relations of the Oneonta sand-

5 (2)

stones and shales to the Ithaca and Portage groups of central New York.

8 Report oF THE STate GEOLOGIST. .

Mr. D. D. Luther, who has already contributed a valuable report upon the
Livonia salt shaft and the products of the salt field generally, has reported
upon the general and economic geology of Onondaga county, and has also
been working upon the stratigraphic relations of the Portage sandstones in
the Naples valley, and along the line of their outcrop from Seneca lake to

Lake Erie.

Dr. Heinrich Ries of Columbia College, has made an elaborate inyestiga-
tion of the geology and economic resources of Orange county, N. Y.,,
contributing much to our previous knowledge of the distribution of the rock
formations in that part of the State. Professor I. P. Bishop, of the State
Normal School at Buffalo, has investigated the structural and economic
geology of Erie county, and has communicated a valuable map showing
the distribution of the geologic formations, and the localities of oil and

gas, with other economic resources of that county.

Professor C. H. Smyth, Jr, of Hamilton College, has been engaged in
the study of the rock formations occupying parts of the counties of St.
Lawrence, Lewis and Jefferson, and has communicated a report upon the
same. Professor Smyth has also made a report on the tale industry of St.
Lawrence county, which will form an important addition to our knowledge
of the economic resources of the State. Professor H. P. Cushing, formerly
of Columbia College, now of Adelbert College, Ohio, has made an examination
of Clinton county, and the adjacent portions of Franklin, and will furnish
a report upon the topography and structural geology of that region.

Professor J. F. Kemp, of Columbia College, has continued his investiga-
tions of the geology and economic resources of Essex county, and this
report, accompanied by maps and diagrams, will form a part of the present
report of the State Geologist.

The following synopses of these several reports and contributions will
give an idea of the nature and results of the investigations carried on in this

department.

7 “ss

SYNOPSES

OF THE: Reowlts OF THE, REPORTS
Communicated by the Several Assistants

me FIELD AND OFFICE, RELATING TO THE
GEOLOGIC MAP OF THE STATE.

The Stratigraphic and Faunal Relations of the Oneonta Sandstones and
Shales, the Ithaca and the Portage Groups in Central New York.

By Joun M. Crarke.

This report presents a revision and summary of observations previously
made by the same author with reference to the position of the Oneonta sand-
stones, and their extent westward from the Chenango river, and adds thereto
more recent data bearing upon the passage of the Ithaca fauna, in the region
of its highest development in Cortland and western Chenango counties,
into the peculiar and typical fauna of the Portage group.

It is shown that the Oneonta group, characterized by its highly colored
beds of shale and sandstone, and of prime economic importance on account of
its high-grade sandstones and flags, lies above an eastern extension of sandy
shales carrying the fauna of the Ithaca group. In the Chenango valley, at
Greene, it is overlaid, at a height of 300 feet, by a fauna having many
strong Chemung features, but in which certain of the Ithaca species are still
present. In the sections along the Genegantslet creek westward of the
Chenango valley, the barren red and green shales are found to alternate with

gray sands carrying the fossils of the Ithaca group and, in a few instances,

_ highly colored shales are observed, in which a few Ithaca species occur.

Over the next divide to the west, and into the valley of the Otselic river,
almost every trace of the red and green beds of the Oneonta group has disap-
peared. It is therefore concluded that the westward disappearance of the
Oneonta group is due to recurrent thinning of the beds, the fossiliferous
Ithaca beds coming in between and dovetailing with them. There is no satis-
factory evidence that the Oneonta beds are followed by a normal Ithaca
fauna, but rather by a fauna whose affinities are decidedly with that of the
Chemung group. The fauna of the Ithaca group is most highly developed
along the valley of the Otselic river and throughout Cortland county.

In making the detailed sections of this group, the base line taken 1s the
Tully limestone, and the sections result in showing outcrops of this limestone
at points considerably south of those previously reported. This is especially
notable along the Tioughnioga valley and in the valley of the Cheningo. In
the Otselic valley the sections of the rocks overlying both the Tully limestone
and the very thin layer of Genesee slate show, first, a series of barren, sandy
shales and flagstones, which are believed to correspond with certain barren

sands lying at the base of the Portage section at Ithaca and some points
11

12 Report OF THE STATE GEOLOGIST.

further west in the more typical Portage region. The same beds are known
to occur further east, and at Sherburne, in the Chenango valley, they were
early termed by Vanuxem, the “Sherburne sandstones.”

Above these le beds of sandy shale, often with considerable quantities
of argillaceous shale, bearing fossils which, for the most part, are Hamilton
species, showing no variation. Gradually, however, forms appear which are
not known to occur in the normal Hamilton fauna, among others Spirifer
mesastrialis, which becomes abundant and large at about 300 feet above the
base of the fossiliferous beds. In the upper portions of the group the fossils
are distributed in thin beds, separated by wide, barren intervals; these barren
sandstones and flags finally predominating to such an extent that fossils are
seldom seen. In the Otselic river section, fossils which occur in the typical
Portage section are very rarely seen; the fauna is a Hamilton fauna, modified
by the presence of some non-Hamilton species, and by certain characteristic
variations of the Hamilton species themselves.

In the Tioughnioga valley, the presence of some of the more abundant
and widespread Portage species is noticeable. The commingling of the two
faunas in the Cayuga lake section is well known. Through Schuyler county,
in sections made at Havana and northward on the west side of Seneca lake,
the predominating fossils are still the brachiopods of the Ithaca group, but
with an increase in the representation of the Portage fauna, which manifests
itself in places in Yates county by some of its indicial types. It is not until
the western limit of Yates county is reached that the normal Portage fauna,
with its peculiar types of life, so distinct from those of the Ithaca group, is
fairly pronounced, and this expression of the fauna is intensified further west-
ward in Ontario and Livingston counties, where evidences of the Ithaca fauna

are met with only at rare intervals.

The Classification and Distribution of the Hamilton and Chemung Series of
Central and Eastern New York.

By Caries 8. Prosser.

These investigations of the rock series from Chenango county eastward
were undertaken principally for the- purpose of tracing the boundaries of
the Oneonta group of sandstones and shales, of ascertaining their stratigraphic
and faunal relations to the deposits above and below, and, also, of elucidating

so far as possible, the division line between the Hamilton group and the over-

Report or THE Stare GEOLOGIST. ts

lying strata and fauna. The latter is a peculiarly perplexing problem. — East
of the Chenango river the Tully limestone and Genesee slate are wanting,
and the sandy shales of the Hamilton group pass upward into those of the
Ithaca group with shght lithologie changes and with alterations of the fauna
so gradual as to be perceptible only upon very careful observation. The Sher-
burne sandstones, of Vanuxem, are shown to be a mass of virtually barren
deposits separating the faunas of the Hamilton and Ithaca groups, corre-
sponding with the lower barren sandstones shown in some sections of the
Portage of western New York, especially at Ithaca, where these beds have
been designated as the “ Lower Portage.” There is good reason for recogniz-
ing this old and well-defined term in application to this mass of barren
sands coming in between the Genesee slate and the overlying fossil-bearing
beds. The term “Sherburne sandstones” would, then, designate an horizon
pretty clearly defined from Cayuga lake eastward into Otsego county or beyond
the disappearance of the Genesee and Tully formations. The rocks in the
Chenango valley sections lying above this horizon, which have heretofore beei
referred to the Ithaca group, are shown to contain a fauna which bears a much
greater resemblance to that of the Hamilton group beneath than to the fauna
contained in the typical exposures of the Ithaca rocks at Ithaca. It is true
that the section at Ithaca is through rocks whose organic content is a com-
mingling of the species more fully and typically represented in Cortland and
Chenango counties, with those which are properly members of the normal

Portage fauna.

The Stratigraphic Position of the Portage Sandstones in the Naples Valley
and the Adjoining Region.

By D. D. Lurner.

The purpose of this work was to ascertain approximately the line of
division between the Portage and the overlying Chemung group in western
New York. The problem is a difficult one, so far as based upon lithologic
grounds, for the rock series consists of sandstones, flags and sandy shales,
varying among themselves. The original upper limitation of the Portage
group, however, was fixed by a mass of heavy bedded sandstones, which
were termed the “ Portage sandstones.”

The author introduces his work by giving a detailed account of a care-

fully studied section of the entire Portage formation in the Naples valley, in

14 Report oF THE STATE GEOLOGIST.

which the precise position of the Portage sandstones is shown and their exact
relation to the faunas of the Portage and Chemung group determined. These
sandstones lie at an elevation of 600 feet above the base of the Portage
formation. A few feet below them is a bed of shales in which are found
characteristic species of the peculiar and distinctive Portage fauna. Between
this layer, however, and the sandstones themselves is a thin stratum bearing a
small fauna unlike anything occurrmg in the normal Portage fauna. This
stratum contains brachiopods (Liorhynchus, Atrypa reticularis, Productella,
ete.), which indicate an encroaching fauna, not distinctively Chemung, but
more closely allied to the Ithaca fauna of the regions east of Seneca lake.

It is further shown that the true Chemung fauna with //ydnoceras
tuberosum and characteristic brachiopods, is well developed within 100 feet
above these Portage sandstones, the intervening rocks not being clearly
exposed in this section, but apparently consisting of barren sandy shales.
The vertical distance from the base of the Portage group to the first pro-
nounced development of a-Chemung fauna, in this section, is less than 760
feet. This is a considerably less thickness than is commonly accredited to this
formation, and much less than that which exists m the typical section on the
Grenesee river at, and below, Portageville, but the former has been measured
with much care, With these data in hand the author has traced the heavy
bedded Portage sandstones eastward to Seneca lake and westward to Lake

Erie.

The Economic Geology of Onondaga County, N. Y.
By D. D. Luter.

In this paper the rock formations are discussed in their proper order of
succession, and while attention is given to the geologic character and dis-
tribution of each, many facts of interest are brought out, and the especial
value of the report consists in its exhaustive treatment of the most
important economic products of this county, viz.: Salt, soda-ash, gypsum,
hydraulic cement and quarry stone.

Following a brief description of the somewhat peculiar topography of the
region, the shales of the Clinton group, the lowest formation represented, are
described. These outcrops are in the low lands of the northern part of the

vara limestone.

county, and have shown no contact with the overlying Niag

The Niagara group is very obscurely developed through the same region east-

Report or tHe Srare Gre YLOGIST. 15

ward, and though quarried at several exposures for local use, it attains no
great thickness and bears but few fossils. The rocks of the Salina group are
shown to be of great importance. Their lower layers, the “red shales,” are
extensively excavated on their exposures, for the manufacture of brick and
tile. This group is also the horizon of the salt brines of this region and of the
rock-salt beds so extensively exploited by the Solvay Process Company in the

vicinity of Tully. A recapitulation is here given of the history of the salt
industry and the mode of production under the control of the State, followed
by an account of the Solvay Company’s soda-ash plant, and a statement
of their process furnished by the company for this report. The facts
brought forward show the enormous industrial importance of the enterprise.
The well records of the nearly forty bormgs put down by this company in
the vicinity of the Tully lakes are discussed and summarized. The impor-
tance of this industry is indicated by the statement that the Solvay Company
consumes 800,000 gallons of brine, 1,000 tons of coal and 1,200 tons of
limestone per day, and gives employment to 3,000 men.

The gypsiferous beds of the Salina group, overlying those containing the
salt, vary somewhat in character, most of the output being from two shaly
layers near the bottom. The history and development of this large industry

is also concisely given, together with its mode of handling, list of producers,

g
_ their output and market.

Under the Lower Helderberg group are considered the productive
water-lime beds. The lower courses of this formation are blue, comparatively
high-grade limestone, largely used for the production of quicklime. The pro-
ductive hydraulic or cement rock les in two beds, near the top of the group.
The mode of quarrying and treating this rock in the manufacture of hydraulic
cement is given at length; account being taken of all the principal producers
and their output. Fossils of Lower Helderberg age are found both above and
below these cement beds.

The Oriskany sandstone is shown to vary considerably in thickness, being

>

actually thicker at the western than at the eastern limit of the county; im one
section within the county totally disappearing, so that the limestones below
come into actual contact with the Corniferous limestone above. It is fossil-
iferous, very interesting from a geologic standpoint, but is of little economic
Importance.

The grand exposures of the Onondaga and Corniferous limestones
render them of great importance to the community. Following an historical

account of the working, is given a description of the usual mode of exploit-

16 Report oF THE STATE GEOLOGIST.

ing and handling, a list of producers and product and of the notable buildings
in Syracuse, affording illustrations of the usefulness and beauty of the rock.

The Marcellus formation is considered, with especial reference to the de-
velopment of the Goniatite limestone.

The shales and sands of the Hamilton group, covering the high lands of
the southern part of the district, are described, and notice. taken of all their
principal exposures.

The Tully limestone, a highly important base line among the formations
in this region, is carefully traced throughout the county and its variations in
thickness measured. It has some value as quarry stone, and its exploitation is
deseribed.

A bed of black shale, overlying the Tully limestone and haying a thick-
ness of 90 feet, is recognized as the continuation of the Genesee slate of
western New York, together with the bituminous shale beds occurring in the
lower part of the Portage formation in Ontario and Livingston counties. As
these black bands within the Portage shales are but sparingly fossiliferous and
their species are for the most part unlike those of the true Portage fauna, the
assumption that the Onondaga county bituminous beds represent the completed
tendency of the ancient seas to such sedimentation at this period may be
probable, while its demonstration from sections would, in the paucity of fossil
remains, be more difficult. The Portage shales and sandstones appear only in
the tops of the high hills at the south, and bear a fauna characterizing the
Ithaca group.

Under the caption, “ Quaternary Era,” the various surface modifications of
the county in late geologic time are considered. In this connection notice
is taken of clay, sand and marl deposits of economic importance, and of the
actual product therefrom.

Following this is a discussion of the condition of the rock strata, with
especial reference to dip, folding and faulting, with citation of illustrative
phenomena ; and much interest attaches to the author's account of the peridotite
eruptive dikes in the city of Syracuse, first discovered by Vanuxem, and
carefully studied in later years by G. H. Williams, and afterwards by Darton
and Kemp.

The report closes with a statistical table of all economic products of the
county, with names of producers and amount and value of output.

The report is accompanied by a geologic map of the county, various

smaller maps, diagrams and sections, and numerous photographs.

Report OF THE STATE GEOLOGIST. 1%

The Structural and Economic Geology of Erie County.
By I. P. Brsnop.

After a brief introductory account of the topography of this region is a
more detailed description of the stratigraphic succession of the rocks. The
lowest rocks are the shales and marls of the Salina group, and the highest,
according to this author’s determination, the upper beds of the Portage group.

Each subdivision is described at considerable length, and features of
special interest are the accounts given of the extensive water-lime beds, the
limestones of the Upper Helderberg division, the Stafford limestone of the
Marcellus shale, the Encrinal lmestone of the Hamilton group, and the
section of the Genesee slate. It is shown that the Tully limestone, which is
absent in all the country west of Canandaigua lake, is here represented by a
layer of pyrite at the top of the Hamilton shales, as shown by D. D. Luther to
be the case in the counties eastward between Erie and Ontario. The section of
the Genesee slate has a thickness of only seventeen feet, about two feet of
this belonging to the Styliola band, which has thus been shown to extend from
Yates county to Lake Erie. The lithologice characters of the Portage shales
and sands are carefully given, but their fossils have received little attention
in this connexion; the upper limit of this formation, in the region
described, is not clearly determined.

Superficial deposits, sands, gravels and clays are treated under the head

? and in connexion therewith is an account of the

of “Quaternary geology,’
soils, springs, pre-glacial rivers and erosion, and the ancient Lake Erie shore
line in Buffalo, This part of the paper closes with a brief notice of modern
geologic changes.

The second main heading is that of economic geology, under which are
considered, first, the rock formations quarried for building stone, viz.; the
hydraulic limestone, Onondaga limestone, Corniferous limestone, Stafford
limestone, Encrinal limestone and Portage sandstones. The interests here
represented are large, as shown by the statistics of producers, and the quality
and amount of the products. Similar consideration is given to the product of
road metal.

Following this is an extended description of the production and manu
facture of hydraulic cement; the nature of the cement rock and a list of its
fossil contents. The production of quicklime, brick, tile, sewer pipe and fire

clays, sand and gravel, is also described at length.
9

18 Report OF THE STATE GEOLOGIST.

A large part of this report is especially concerned with the product of
natural gas and records of the wells which have been drilled in and
about the city of Buffalo. This account has been prepared with elaborate
care, giving a full list of the gas-producing companies or individuals, their well
records and product. The tabulated list of wells, productive and non-
productive, embraces sixty-seven. These statistics are supplemented by some
discussion of the geology and supply of natural gas. Brief accounts of the
rock salt and water power of the county are followed by the description of
a general geologic section from Lake Ontario to Cattaraugus creek.

The paper is accompanied by a geologic map of Erie county, with several

maps showing the location of the gas wells, and by numerous photographs.

Report on the Geology of Orange County.
By Heryricn Rres.

The introductory parts of this report are devoted to a description of the
physical geography and topography of the region, followed by a summary of
geologic literature pertaining to the district.

The geologic formations present are then taken up in consecutive order
for brief discussion.

The pre-Cambrian rocks are largely developed, consisting of gneisses,
gneissoid rocks and limestones, all frequently traversed by dykes of igneous
rock. The bodies of iron ore which are worked in this county lhe in these
crystalline rocks.

The Cambrian rocks are light colored, generally heavy bedded magnesian
limestones, and though apparently without fossils, they seem to be a con-
tinuation of the limestones of northern New Jersey, in which fossils have
been found. These limestones frequently become crystalline as a result of
granite intrusions.

The Trenton group is represented only by a single exposure near New-
burgh. The Hudson river shales and sandstones are very widely extended
and cover nearly two-thirds of the area of the county. In a few localities
they have furnished fossils. In the Shawangunk mountains, the Medina sand-
stone has a thickness of about fifty feet in the town of Deer Park, and “also
appears in the vicinity of Skunnemunk mountain. The Lower Helderberg
series appears at several points, and at the best exposures its different mem-
bers can be determined. The Oriskany sandstone and quartzite occurs in two

Report oF tHE SrateE GEOLOGIST. 19

belts, one passing through Port Jervis, and the other along the western side
of Skunnemunk mountain. The Cauda-galli grit, “Esopus slate,” as it has
been termed by Darton, rests on the Oriskany in eastern Deer Park town-
ship. Outerops of the Corniferous limestone are restricted to localities near
Port Jervis and Port Orange, its thickness being estimated at 250 feet. The
Hamilton group is well developed in the county. The Marcellus shales are
seen along the Neversink valley, and are estimated to attain the enormous
thickness of 800 feet. Overlying them in the same region are arenaceous
shales of the Hamilton group with a thickness of 1,800 feet. A second area
of Hamilton rocks in the Skunnemunk mountain region has been separated
into local subdivisions, viz.: the Monroe shales, Bellvale flags, and Skunne-
munk conglomerate. The Chemung formation caps the rock section, and is
represented by non-fossiliferous beds in the western portion of Deer Park.

Following this summary statement of the distribution of the geologic
formations, the author enters more explicitly into a discussion of the geologic
relations of each, and more detailed accounts of their areal extent. The
following captions show the general mode of treatment: Geology of the
Warwick Cambrian limestones, and the granites; Relations of the limestones
and Hudson river slates; Geology of the region along Bellvale mountain ;
Pre-Cambrian gneiss; Geologic relations of the area along Skunnemunk
mountain; The relations along the northwest side of Skunnemunk mountain ;
Geology of the region east and southeast of Skunnemunk mountain; The
area west of Cornwall; Geology of Deer Park township; Hudson river slates
and sandstones; The Neelytown limestone; Geology of Newburgh and New
Windsor townships; The Highland area of gneissic rocks; Tuxedo township,
Monroe township, Woodbury township, Highland township, Cornwall town-
ship; Dike rocks; Quartz porphyry; Pleistocene geology.

These chapters, each of which is elaborated in detail and_ precision,
precede a special consideration of the economic geology of the county.

The various materials available for road making are described; brick
clays, their quality, workers and product; limestone, lead ore, building stone,
flagstone, iron ores and their workings, handling and product, are fully con-
sidered - and, finally, the soils, mineral springs, water power and water supply.

20 Report oF THE STATE GEOLOGIST.

Report on the Talc Industry of St. Lawrence County.

By C. H. Smytu, JR.

In a previous report the author had given some consideration to a certain
portion of the tale deposits in this region. A fuller account of the talc, its
nature, occurrence and exploitation is here presented. The deposits of this
mineral are largely in the towns of Edwards and Fowler. It may occur at
several horizons in beds of considerable thickness, and it is evident that these
beds are intimately related to the crystalline limestones with which they are
associated. The walls of these tale beds consist of a tremolite rock passing
gradually into the limestone, and one evidence that the tale is derived by
gradual alteration from the tremolite is the fact that much of the mineral is
distinctly fibrous, a condition of first importance to the economic applications
of the tale The soft, scaly, non-fibrous tale is regarded as the ultimate
condition of the mineral resulting from the continuation of the decompo-
sition of the tremolite. Some account of the number of mines is given,
followed by a description of the process of manufacture, and some discussion
of the value of variations in physical character of the mineral, and finally a

statement of its uses In manufactures.

Report on the Crystalline Rocks of St. Lawrence County.
By C.. H. Smyrtu, Jr.

This is an account of work done in this county in continuation of obser-
vations already made in a previous report. The townships whose geology is
especially considered are those not canvassed in the previous survey by the
author. The principal purpose of the work has been to determine the distri-
bution of the crystalline limestones, for which the writer had already intro-
duced the term, “ Oswegatchie series ;” and, also, to collect data bearing upon
the question of the origin of the gneisses and the relation existing between
these rocks and the limestones. The limestones occur principally in belts, as
well as in small scattered patches. The extent of these limestone areas is
described, and in the same connection the areal distribution of the gneisses.
Three or four distinct belts of limestone are defined, together with smaller
accessory areas. The limestones are highly crystalline, with a considerable

range of color, and carry masses of embedded silicates, among them tremolite

Report oF THE State GEOLOGIST. 21

in such abundance as sometimes to constitute a tremolite schist. Interbedded
with the limestones are, sometimes, gneissic rocks. The author infers that the
limestones, having their greatest development in the northwest part of the
county, decrease rapidly in passing southeastward toward the heart of the
Adirondacks.

Under the heading, “Origin of the Gneisses,” the two important
problems are discussed—the origin of the gneisses, and their relations to the
limestones. In considering the first of these, three explanations are presented
as possible, and worthy of consideration ; the first, that the gneisses are meta.
morphosed sediments; the second, that they are of igneous origin; the third.
that they are partly metamorphic and partly igneous. It is shown that the
principal evidence in favor of the first hypothesis lies in the association of
the limestones with the gneisses, but this is regarded as insufticient to prove
that the gneisses belong to the limestone series. The second hypothesis is
considered in much detail. Evidence in its favor is found in the general
foliation of the gneisses, and in the microscopic structure of the rock aftord-
ing various evidences of pressure, flow, and secondary changes. Facts are
brought forward to show that the gneiss contains masses which are inclusions
of some older formation, perhaps taken up by the gneiss when it was in a
molten state.

As the author does not regard the gneisses and the limestones as parts
of one series, the former must be older or younger than the latter, and he
believes that the gneiss is, in part at least, the younger, and instances are cited
where the gneiss appears to be intrusive into the limestones, and accompanied
by local metamorphic contact effects. With regard to the general relations of
the gneisses and limestone, it is concluded by the author that the gneisses
constitute a complete series of rocks, differmg somewhat in age, and largely,
if not almost wholly, of igneous origin; that parts of this series are younger
than the limestones ; and while it is possible that other parts may be older
than the latter, there is, however, no absolute proof of this assumption.

Report on the Geology of Clinton County.
By H. P. Cusuine.
After a general presentation of the topography of this region, the author
fon) fo) . fo)
takes up for especial consideration seriatim the geologic formations, as

follows:

bo
bo

Report OF THE STATE GEOLOGIST.

1. Gneissic series; 2. Limestone series; 3. Gabbro series; 4. Palaeozoic
series: (@) Potsdam sandstone, (>) Calciferous sandrock, (c) Chazy lime.
stone, (7) Black River limestone, (¢) Trenton limestone, (7) Utica slate;
5. Dike series; 6. Pleistocene deposits.

Then follow important chapters on the metamorphism of the Pre-
Cambrian Rocks and on Post-Champlain (Lower Silurian) Disturbances.

The latter half of the paper is devoted to the discussion of the areal
geology by townships, in the following order:

Clinton, Mooers, Ellenburg, Dannemora, Saranac, Black Brook, Ausable,
Peru, Schuyler Falls, Plattsburg, Beekmantown, Altona, Chazy, Champlain,

Preliminary Report on the Geology of Essex County.
By J. F. Keye.

This report is a continuation of the author’s geologic investigations,
published in the report of the State Geologist for 1893. Townships not
previously described are taken up for special consideration and descrip-
tion, and the areal geology of each is given, so far as determined. Special
notice is taken of economic products, mainly of iron ores.

In the town of Chesterfield, so far as explored, the gneisses are extensively
developed, but no new facts in regard to other series of rocks have been
obtained since the last report.

In Jay, the gneisses constitute the northeastern corner; the crystalline
limestones occur in upper Jay, and constitute the northerly continuation of
the area of similar rocks occurring in Keene; rocks of the gabbro family
cover the main portion of the town, while no palaeozoic sediments or dikes
of irruptive rocks have been observed.

In Wilmington, the gneisses and gneissoid rocks with crystalline lime-
stenes are believed to be absent. The entire eastern portion of the town is
covered with gabbros and anorthosites, while no sedimentary rocks are found
in the town. <A single trap dike is observed at the high falls of the West
Branch of the Ausable.

St. Armand. The gneisses are well represented, but the crystalline lime-
stones and their associated rocks are not met with in the town. The area of
gabbros, represented on the map largely from inference, appears to be con-
siderable. No palaeozoic or irruptive rocks have been noted.

Report OF THE STaTE GEOLOGIST. 23

In North Hudson, so far as explored, only the gabbros have been noted.

In Schroon, the gneisses and crystalline limestones cover almost the entire
township except the northern portion where there are gabbros, and a small
area at Schroon Lake post office, correctly regarded as Calciferous sandrock.
The last is the remotest outlier yet observed of palaeozoic sediments in the
mountains. Several dikes are noted; one at Pharaoh pond, others west of
Schroon Lake post office. Iron ore occurs in the Schofield bed at the extreme
east of the town.

Minerva is chiefly covered with gneisses and crystalline limestone; on
the northeast, gabbros and related rocks occur, and the same are present along
the eastern border. No palaeozoic rocks or dikes were met with. There is
little iron ore in the town, and garnet is worked at one locality for an abrasive.

Newcomb has been but partially studied. The gneisses and crystalline
limestones are widespread; the folding of the latter has been an important
factor in producing the lake basins in the central part of the town and in de-
termining the water courses. The anorthosites and gabbros make up the
eastern third of the township. No palaeozoic rocks or irruptive dikes have
been observed in the town. In the vicinity of lakes Sandford and Henderson
are extensive iron mines. These mines were opened at the village of Me-
Intyre and bloomeries established about 1835, by the late Hon. Archibald
MelIntyre. A very complete history of their workings, with a description of
the ores, analyses, and a map of the mines, are given. The amount of ore in
sight is enormous, and though highly titaniferous, it is thought that it may be
profitably worked with the revival of the iron demand and an improvement
in shipping facilities.

The geologic notes made upon the separate townships are often in con-
siderable detail, involving careful analyses of rock structure and derivation.

Thickness of the Lower Silurian Formations along West Canada Creek and
the Mohawk River.

By Cuaries 8. Prosser and Epear 8. Cumryes.

The writers here consider nv extenso the rock sections exposed in the
gorge of the West Canada creek at Trenton Falls, at Newport and at Little
Falls.

These sections have all been previously studied by other observers, some

of them frequently, and not always with concordant results. In this paper,

24 Report OF THE STATE GEOLOGIST.

both measurements of thickness, and identification of species of fossils haye
been made with care, and while the conclusions are not in complete harmony
with already expressed opinions, they doubtless afford a more vrecise knowl.

edge of the formations considered.

PALAEONTOLOGY.
Note on the Discovery of a Sessile Conularia.
By R. Rurepemann.

This important paper by Dr. Ruedemann, who contributed to the report
of last year an interesting memoir on the Graptolites, is based upon the study
of some obscure organisms found in the Utica slate at Dolgeville, N. Y.
Portions of this paper have already been published during the past year in
the American Geologist, and they make so significant a contribution to our
knowledge of the fossils of this State that, with the author’s consent, these
portions are here reproduced with their accompanying plates. To these are
added further observations and illustrations. As a result of this study much
light is thrown upon the nature and mode of development of this wide-spread
but little understood organism, Conularia, in regard to whose taxonomic

position there has been a widely diverse expression of opinion.

A Discussion of Streptelasma and Allied Genera of Rugose Corals.
By James Hatt.

The genus Streptelasma has never yet been clearly defined, and thus the
nomenclature assigned to it has been one of general and conventional use.
The entire group of American species which have been referred to this genus
are here brought together and their structural characteristics carefully
analyzed. It has been found that the term Streptelasma must be carefully
restricted to forms like the Si corniculum, Hall, of the Trenton fauna. Devia-
tions from this type of generic structure are here recognized under distinct
designations: Thus the S. mammifer, Hall, of the Upper Helderberg lime-
stone, S. caliculum, Wall, of the Niagara group, and S. rectum, Hall, of the

Hamilton shale, aré each made the type of a distinct genus. A new form

%y

Report oF THE STATE GEOLOGIST. 25

from the Trenton limestone is described as Streptophyllum cystosum. A new
species from the Hamilton group is, as Lopholasma carinatum, made the type
of a new genus. The Petraca Hanningani, of Safford, is likewise made the
type of a new genus. The genus Duncanella, Nicholson, is also reviewed,
additional structural features determined, and some new specific forms
described. The paper is accompanied by a lithographic plate and numerous
text illustrations

The Palaeozoic Hexactinellid Sponges Constituting the Family
Dictyospongide.

Part I.

This work was communicated with the annual report of last year, but on
account of its necessarily extensive illustration, the State printer was deterred
from producing it. The appreciative co-operation of the Wynkoop Hallenbeck
Crawford Company, the present State printers, and the endorsement of the
Hon. James A. Roberts, Comptroller of the State, have made its publication
at this time possible. It is proposed to present with this report that portion
of the work concerned with the general introductory discussion of the nature
and structure of these interesting fossils, and the description of such species
as are known to occur in the Silurian and Deyonian formations. This will be
followed, in the next annual report, by accounts of other representatives of
this family occurring in the faunas of the lower Carboniferous formation.
This arrangement will make possible the publication of the one thousand
separate copies of this monograph which are called for by Chapter 932 of the
Laws of 1895, without serious delay.

The Dictyospongide constitute a family of thin-walled, reticulate, siliceous
sponges whose life, so far as known, was restricted to palaeozoic time. The
first of these fossils to be described was regarded as a Cephalopod and termed
Hydnoceras (Hydnoceras tuberosum, Conrad. Journal Philadelphia Academy
Natural Science, vol. vill. 1842); subsequently this and other species were
interpreted as remains of marine algw and a few species from the later
Devonian rocks became pretty well known to collectors of New York State
fossils. Their real nature was recognized about fifteen years ago by Prof.
R. P. Whitfield, from the study of specimens found in the soft calcareous
shales of Crawfordsville, Indiana, which retained the spicular skeleton of the
sponge in the condition of iron pyrites.

26 Report oF THE STATE GEOLOGIST.

In this memoir an effort has been made to bring together all that is now
known concerning this remarkable family. The work is based upon the
result of more than fifty years of care and watchfulness in securing the mate-
rial which is here illustrated, and more than once during this period it has
seemed as if the end of these resources had been reached, but in every case
new forms have come to light. Explorations carried on in late years, in the
Chemung rocks of this State, especially by Mr. E. B. Hall, of Wellsville,
Allegany county, have shown a most surprising development of these
fossils and we have good reason to believe that, notwithstanding the fre-
quent occurrence of living hexactinellid sponges in existing seas, the
Chemung period was the time of culmination of the entire order Hexac-
tinellida, to which this family belongs. At the present time more than
seventy species of these Dictyosponges have been recognized in the Chemung
fauna alone, and we have been able to locate areas where they grew in
colonies or plantations on the sea bottom of that ancient period. In previous
faunas they were much fewer, and in those succeeding the Chemung, they
continued for only a brief period, though with most interesting manifestations
of form and structure. This memoir will embrace descriptions and illustra-
tions of over one hundred and twenty species, at present recognized under
twenty-nine genera.

Very respectfully, your obedient servant,
JAMES HALL,
State Geologist and Palacontologist.

GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

(GEOLOGIC MAP.)

THE STRATIGRAPHIC AND FAUNAL RELATIONS OF THE
ONEONTA SANDSTONES AND SHALES, THE ITHACA AND
THE PORTAGE GROUPS IN CENTRAL NEW YORK.

JAMES HALL, | JOHN M. CLARKE,
State Geologist. | Assistant State Geologist.

1895.

: ee 4

, iy Wee ee &

James Hatt, State Geologist.

Srr:—The report herewith submitted is in continuation of that made
by me in the Thirteenth Annual Report, and concerns the inter-relations of
the various geologic deposits laid down during Portage time, especially as
developed through the central region of the State. The stratigraphy and
faunal succession in Chenango county, west of the Chenango river, have been
previously discussed in some detail. Here I have endeavored to correlate
those observations with such as have since been made further westward

_ through the counties of Cortland, Schuyler and Yates.

Respectfully yours,
JOHN M. CLARKE.
Apany, January Ist, 1896.

PLATE |

QO

WyNKOOP HALLENBECK CRAWFORD C

The Stratigraphic and Faunal Relations of the Oneonta
Sandstones and Shales, the Ithaca and the Portage
Groups in Central New York.

By Joun M. Crarke.

In the Thirteenth Annual Report of the State Geologist, dated 1894,
the writer communicated the preliminary results of observations made in
Chenango county, with especial reference to the westward extension through
that region of the barren sandstones, red and green shales constituting the
Oneonta beds, as defined by the late Lardner Vanuxem. Sufficient evidence
was there brought forward to show that westward of the Chenango river
this group of beds, so important economically for its high-grade sandstones
and so strikingly characterized by the brillant coloration of many of its softer
beds, rapidly thins out. Even before reaching the western limit of Chenango
county the last positive evidence of it has disappeared. The Genegantslet
creek, a considerable water course rising in the high land of Pharsalia town-
ship and flowing almost due south into the Chenango river, gives a number
_of instructive sections which offer a clew to the mode of its disappearance.
The entire mass of this distinctly eastern sediment does not thin to a single
edge. Between it and the contemporaneous sediments of the fossil-bearing
Ithaca group, which predominate in western Chenango county, there was a
constant oscillation and a mutual encroachment; consequently the rock
sections show recurrences of Oneonta conditions after the main body of such
deposits had been left far below. Thus, in the village of Greene, on Bird-
sall’s brook (Station M, Report of 1894), a section lying almost as low as the
river level in the Chenango valley, the characteristic Oneonta shales and
sands, with their reds and greens, are well shown. But northward along the
Genegantslet, flowing through high lands well elevated above this spot are
repeated evidences of such highly colored beds, separated from those beneath
by intervals of fossiliferous rocks. At Station N, two miles north of Greene
on the highway to Smithville Flats, are fossiliferous shales, 150 to 200 feet
higher than the beds at Station M; at Station O, two and one-half miles north
of Smithville Flats and considerably higher in the section, are again green shales
and sands with fish remains, a repetition of the Oneonta sediments, together

with shaly layers bearing fossils. Still further north, a short distance south
31

32 Report OF THE STATE GEOLOGIST.

of the village of McDonough, and still higher in the section, are fossil-bearing
rocks, and in the town of Pharsalia (Stations T, T', T?), at about the same
elevation in the section, there lies, above certain fossiliferous beds, a peculiar
fawn-colored cavernous sandstone which reproduces an Oneonta character,
inasmuch as a similar rock has been elsewhere observed, only with typical
Oneonta sediments at Station E, near Norwich. Westward of the Gene-
gantslet valley, evidences of these Oneonta beds may exist for a short distance
into the divide between the Genegantslet and Otselic rivers, but they have
not been observed in the valley of the latter stream. Traces of such red and
green beds may naturally be expected westward in Cortland county, inter-
calated among the deposits properly belonging to the Ithaca group, but none
have been seen by me. Such instances as those quoted serve to show that the
Oneonta deposits disappear westward both by thinning and recurrence, not
contracting to a single edge, but dovetailed by a number of edges or long :
planes into the sediments bearing the Ithaca fauna. No recurrence of these
beds in the easterly region, where their development is pronounced and
typical, has been recorded.

In the region along the Chenango valley, where the Oneonta beds have
not been penetrated by the straggling representatives of the western fauna,
opportunity is afforded of studying closely the important question as to the
composition and nature of the fauna succeeding the body of the Oneonta
deposits. This matter has already been referred to in my preliminary report,
and since then additional evidence has come into my hands which I shall take
the opportunity of presenting at this point.

In the report referred to, attention was called to the outcrops on Juliand
hill (Station K) in the village of Greene. ‘The first exposure here is about
150 feet above the Chenango river and not less than 100 feet above the top
of the Oneonta beds as exposed on Birdsall’s brook. Several species were
recorded from the various exposures on the hill, which individually and collec-
tively give a decided Chemung expression to the fauna. The principal of
these were: Schizophoria impressa,; <Atrypa reticularis, very large form ;
Liorhynchus globuliformis ; Leptostrophia perplana, var. nervosa. 1 take
occasion to correct, with the help of added material, two identifications then
made, namely: Spirifer mesastrialis and Productella ef. lachrymosa. The
former of these proves to be a varicose, narrow-winged shell of the S. mucro-
natus type, strikingly near the normal form of the species as it occurs in the
Hamilton group. Further notice will be taken of it presently. The other

species is a rather large form of Productella speciosa.

CLARKE—OneEontTA, ITHACA AND PorTaGE Groups. 33

The desirability of having this Juliand hill section more fully elaborated
has led me to request Mr. F. H. Williams, of Greene, a very careful observer,
to collect the desired data for me. Mr. Williams, at the expense of some time
and no little labor, most cordially responded to my application, collecting with
much care from all exposures, not only on Juliand hill, but also on the
neighboring Cowles hill, and in a ravine known as Flag Gulf, about three
miles south of Greene.

It will be observed that these sections serve to fortify the conclusion
previously drawn in regard to the character of this higher fauna. Certain
Chemung traits are evident therein, notwithstanding both the absence of some
distinctive Chemung types and the presence of some continued Ithacan features
The fauna is doubtless one of those passage groups which, in easy rock sue-
cessions, cannot be referred with precision to either the preceding or the
following fauna except upon a careful weighing of the predominant traits.
Here the majority of organic characters points to a closer alliance with the
later (Chemung) fauna than with that which has been left below.*

Juliand Hill. (Figure 1.)

The first outcrop (A) is at an old quarry 150 feet above the Chenango
river, probably 75-100 feet above the Oneonta green sands and shales exposed
on Birdsall’s brook, Greene (Station M, Report 1894). The rock is a flaggy
gray sandstone, with the following fossils :

Atrypa reticularis. This is the very large, expanded and gibbous form
common at certain Chemung horizons in the western counties. It is here
abundant and associated with smaller specimens of relatively coarser plication ;
undoubtedly young forms of the same variety.

Tentaculites spiculus.

Spirifer mucronatus var. A diminutive form, short winged, faintly vari-
cose and with but a trace of the median plication at the bottom of the sinus.
It is a distinct departure from any expression of this species occurring in the
Hamilton group, and is probably identical with the variety posters.

Actinopteria eta.

Goniophora sp.

* Sueh introductory fannas, preceding the culmination of a given organic assemblage, though they may embarrass the sub-
division of sedimentary formations and obscure lines of demarkation, especially where, as in this State, the succession is
undisturbed, yet involve many importantt questions pertaining to the history of organic life and the bathymetry of ancient seas.
In another place the writer has used the expression, prenunczal fauna, for one which appears abruptly and in partial development,
and after & brief sojourn disappears, to reappear in the same vertica! section after a considerable interval and in fuil form. Thus

. the fauna of the Genundewah or Styliola limestone of the Genesee beds in western New York is prenuncial of the Naples fauna,
from which it is separated by a mass of bituminous shales, with but few fossils, and those of but little similarity to the members
of adjoining faunas. For an introductory fauna which heralds the incoming of a new organic association and passes gradually,
Without interval or interruption, into that culminant assemblage, the term proemiad fauna may appropriately be used.

3

34 Report oF THE STATE GEOLOGIST.

Poteriocrinus sp.

B, a short distance above, exposes avout fifteen feet of a sandy shale with

Schizophoria impressa, very large and highly convex: abundant.

Atrypa reticularis, as above ; common.

Spirifer mucronatus, small variety, as above.

Leptostrophia perplana var. nervosa.

This shell is somewhat smaller and of less irregular form than in its
occurrence in the Chemung of the southwesterly counties. This difference in
the early and later forms of this variety has already been adverted to by

JULIAND HILL
Greene WY.

From a pection furnished by

FLW. Williams

FIGURE 1.

Professor H. 8S. Williams, who speaks of the Chemung form as the “ coarser
and more irregular.”

Tentaculites spiculus.

Actinopteria eta, common.

At C and C’, fifty feet higher, are two exposures of sandy shale separated
by about six feet.

Schizophoria tmpressa, as above ; common.

Atrypa reticularis, as above; common,

Productella SPeCiOSd, common,

Actinopterta etd.

Microdon gregarius.

Spathella typica.

Grammysia elliptica,

Bellerophon Maera. ‘This shell is somewhat smaller than the usual form

of the Chemung fauna, and its surface pustules do not always extend to the

CLARKE—OwneonTA, IvHaca anp Portage Groups. 35

aperture ; in some specimens a considerable portion of the apertural part of
the body whorl is smooth.

Cyclonema multilira (obsoletum ?).

D, fifteen feet above, affords an exposure of two to three feet of flags
with :

Stropheodonta demissa, large and fine examples of the characteristic Che-
mung form with finely divided plications, obliquely undulated cardinal slopes
and extended cardinal extremities.

Atrypa reticularis, as above; common.

Schizophoria impressa, with ventral valve highly arcuate.

Productella speciosa.

Actinopteria eta.

Cryptonella.

E, at the summit of the hill, twenty feet above, contains :

Atrypa reticularis, as above. 5

Liorhynchus globularis. The original specimens of this species of Van-
uxem’s seem to have come from Otsego county. Iam not aware that the
species has been recorded in faunas of whose Chemung age there is no
question.

Tentaculites spiculus.

This is a repetition, with some important additions, of the fauna pre-
viously made out by me in these rocks. The top of the hill les about 300
feet above the Chenango river and the rock section here given is, thus, through
150 feet, approximately.

Cowles Mill. (Figure 2.) The section at the Cameron quarry, in this
hill, has been referred to as Station L of my preliminary paper. Mr. F. H.
Williams has examined the entire section from this old quarry, mentioned by
Vanuxem in his report of the Third district (1842), and which les near the
base of the hill, upward to its summit, an interval of about 350 feet. Cowles
hill lies in the southwest portion of the village of Greene and about one-half
mile due south of Juhand hill.

1, The Cameron quarry, approximately 100 feet above the Chenango
river. Here, at the base, are ten feet of compact sandstones, with a concre-
tionary layer near the top, and above, in the same exposure, forty feet of
arenaceous shales.

The fossils collected are :

Tentaculites spiculus. Vanuxem refers to the abundance of Tentaculites

at this spot.

36 Report oF THE SratreE GEOLOGIST.

Microdon gregarius.

Grammysia elliptica.

Actinopteria eta.

Atrypa reticularis, large, as above.

Schizophoria impressd, large, as above.

Spiriter mucronatus. ‘This is a form of the species which presents the
characters normal to the typical form; delicately varicose surface, well
defined median plication at the bottom of the sinus, and narrow, considerably
extended wings.

Cyrtina recta.

Spiriter mucronatus. The small, short-winged variety mentioned above.

Productella speciosa.

Liorhynchus globuliformis.

é softest
== 1 enw dony)
fe gs COWLES HILL
-Greene, NY
J Section furnished by FH Williame

gn

FIGURE 2.

2, Is ninety feet higher up; sandy shales, containing:

Atrypa reticularis, very abundant.

Schizophoria vmpressa.

Liorhynchus globuliformis.

Spirifer mucronatus, both the normal form and the variety above men-
tioned.

3. Calcareous and arenaceous shales, sixty feet above.

Spiriter mucronatus. The small variety above mentioned ; abundant.

Schizophoria impressa, large.

Productella speciosa.

Atrypa reticularis, large.

CruarKE—OwneronTA, IrHaca anp Portrack Groups. Sif

Stropheodonta demissa, the Chemung variety.

Liorhynchus globuliformis.

Leptostrophia mucronata.

Spirifer levis.

4, Is 175 feet higher and twenty-five feet below the summit of the hill.
The rock exposed consists of sandy shales, with some soft olive shale inter-
ealated. Fossils are apparently abundant, and the following have been iden-
tified :

Lyriopecten cf. interradiatus. This shell is usually of small size and, on
the whole, is nearer to the form suggested than to LZ. tricostatus. It will be
observed that the normal form of the latter species is present in the Flag Gulf
section given below. The two species differ only in the number of finer inter-
calary ribs between the principal plications; these in LZ. interradiatus are few,
sometimes no more than a single one, but in L. técostatus they may number
three to five. The former species has thus far been recorded only from the
shales of the Hamilton group at Fultonham, Schoharie county, while Z. ¢r7-
costatus, though generally found in the normal Chemung fauna, occurs in
undoubted Hamilton beds at Summit, Schoharie county, where it is associated
with Chonetes syrtalis.

Schizodus Chemungensis.

Actinopteria of the type of Boydi, eta, etc.; much larger than the pre-
vailing form of the latter, with very distinct surface characters; probably a
distinct species.

Spathella typica.

Paleoneilo ct. plana.

Paleoneilo cf. muta.

Grammysia cf. communis.

Bellerophon Maera.

Pleurotomaria cf. Itys ; a variety.

Schizophoria impressa, as above.

Atrypa reticularis, as above.

Productella speciosa.

Stropheodonta demissa, as above.

Spiriter mucronatus, both forms as above mentioned.

Spirifer levis.

Species of especial interest in the last two localities are Leptostrophia
mucronata and Spirifer levis. The former is abundant in a thin calcareous

layer, is uniformly of small size, and though without mucronate cardinal

38 Report OF THE Srare GEOLOGIST.

extremities, bears all the characters distinctive of the common expression of
the species in its occurrence through the Ithaca fauna of Cortland, Tompkins
and Schuyler counties. The mucronate extension of the hinge is by no means
a persistent feature of typical forms; indeed, the name itself was based upon
forms in which this extension is but slight, and it is not unusual to meet with
individuals in which there is no evidence of any lateral prolongation of the
hinge angle; the condition of the shells at the horizon under consideration.
But this mucronation of the shell may be carried to a great extreme and afford
unprecedented illustration of such configuration among the stropheodontoid
brachiopoda. A specimen from Spafford, Onondaga county, 3875 feet above
the Tully limestone and associated with Zornoceras uniangulare, Buchiola
speciosa, Paracyclas lirata, etc., bears at each angle a curving cardinal spine

having fully as great length as the shell itself (Figure 3). Several specimens

FIGURE 3. Leptostrophia mucronata, Conrad (sp.). Spafford, N. Y

from that locality all show the same character. Close analysis of this feature
is needed to show whether its variations possess a definite local or time value.
Suffice it to say that in all observed specimens from the Cowles hill section
the shells are small and the angles not produced.

Of the specimens referred to Spirifer evis, nine have been seen from the
two stations 8 and 4. These are, for the most part, internal casts, one a cast
of the exterior affording the superficial characters of the shell, and one or two
partially exfoliated shells. Upon careful comparison of these specimens with
the species as it occurs at its typical locality, Ithaca, involving close analysis
of all the structural characters that can be made out, there remains but a
single palpable distinction ; the Cowles hill specimens are uniformly smaller.
This may be a difference of significance in consideration of the great time
interval in their appearance, but with a reservation in favor of this point only,
[ unhesitatingly refer the forms under consideration to that specific type.

The reappearance of this species is the more interesting as in the Ithaca
meridian it is best developed at a well-defined horizon near the base of the
entire Portage sediment, where it is highly abundant, but strongly localized.

Professor Williams has recorded its bref recurrence in this meridian after

CLaARKE—Owneronta, ITHAcA AnD Porrace Groups. 39

the withdrawal of the Ithaca fauna, about 500 feet higher in the strata.*
Aside from the occurrence about Ithaca and that at Greene the species has
been found, I believe, only at Hait’s quarry near Homer, and (as recorded
on a later page of this paper) near McGrawville, Cortland county ; in both
instances with but few specimens.

This reappearance of Spirifer Jevis at an horizon which cannot be less
than 1,200 feet above its first appearance and most profuse development in
the rock series of the Ithaca section, and several hundred feet above its last
appearance in that section, is remarkable and unexpected. Its association with
Leptostrophia mucronata shows that, as we have already suggested, the Ithaca
fauna is not yet wholly extinguished, though its relicts are here consorting
with predominant and more and more emphatic Chemung types.

Their presence in this association can no more modify.our conception of
the post-Portage age of this fauna than if they were altogether absent, or,
rather, the fact of their presence here, under certain structural modifications,
is very evidence of such age.

Flag Gulf (Figure 4). This is a ravine lying three miles south of Greene
on the east side of the Chenango river. The succession of rocks and fossils
is as follows:

The lowest exposure (]}) is about seventy-five feet above the river and
consists of gray flags; no fossils observed.

Above this are three feet of soft shaies (2), followed by four feet of sand.
stone (3); no fossils were found here.

At (4) are five feet of flags and shales containing :

Schizophoria impressa, large form.

Productella speciosa.

Spirifer mucronatus, small variety.

Above (8) are six feet of soft shales with Spirfer mucronatus, small
variety.

Leptostrophia perplana, var. nervosa, typical Chemung form.

Actinopteria eta.

At (6) are twelve feet of sandy shales with but few fossils, namely :

Actinopteria eta.

Goniophora minor.

Spiriter mucronatus, small variety.

* Mr. E. M. Kindle, in a publication entitled *‘ The Relation of the Fauna of the Ithaca group to the Faunas of the Portage and
Chemung,” (Bull. Amer. Paleontology, No. 6, dated December 25, 1896) mentions the occurrence of this species at an horizon 130
feet below this upper 9. Jevis zone (p. 86) and refers to the abundance of the fossil at its later appearance (p. 29). See further note
on this paper on page 57.

40 Report OF THE STATE GEOLOGIST.

Then follow five feet of shales (7) with

Schizophoria impressa, large and medium.

Spiriter mucronatus of typical form, long winged and with varicose
surface.

Lyriopecten tricostatus, the typical Chemung form.

The rocks above this for one hundred feet (8) are covered with gravel;
then follows an exposure of fifteen feet of soft shales (9) with

Productella speciosa.

Stropheodonta demissa, Chemung var., abundant.

Schizophoria impressa, large.

Liorhynchus globuliformis, common.

Atrypa reticularis, large form.

Actinopteria eta.

FLAG GULF

Smiles 6 of Greene, NY. Te)
* Section furnished by FHWilliams. “

FIGURE 4,

The next sixty feet above (10) are covered, then follows (11) an exposure
of about forty feet of flags, sands and shales in an old quarry which was
worked about sixty years ago. These rocks have afforded

Productella speciosa, common

Schizophoria impressa, as above.

Spiriter mucronatus, norma.

Liorhynchus globuliformis.

Atrypa reticularis.

Lyriopecten tricostatus, as above.

CiarkKE—Oneonta,- IrHaca AND PortacEe Groups. 4]

Bellerophon Maera.

From this quarry it is about seventy-five feet to the top of the hill, and
the exposures in this distance have not yet been examined by Mr. Williams.
The total height of the hill proves from the measurements given in this see-
tion to be about 400 feet.

It is clear that the same fauna permeates all these sections. If we allow
150 feet for the southeriy dip of the rocks in the interval of three miles
between Juliand hill and Flag gulf, the lowest outcrop on the former will be,
approximately, just below that first appearing in the Flag gulf, so that our
former section is essentially reproduced in the latter, with an upward addition
thereto of 250 feet. These consecutive sections give us evidence of a Chemung
fauna antedating the Spirifer disjunctus fauna, and extending through at least
400 feet of strata.

It is necessary to observe that the lower horizons of this essentially
homogeneous fauna lie no higher above the Oneonta beds than do some of the
smaller, quite distinct faunules which manifest themselves at intervals in the
hills bounding the Genegantslet creek, northward to the village of McDonough.
But all of the latter are much less firmly characterized by such distinctive
Chemung types. In these outcrops are observed such species as the following:
Spiriter mucronatus var. posterus, Grammysia elliptica, Sphenomya subcuneata,
Leptodesma Logersi, Leda diversa, Camarotechia congregata, Goniophora
subrecta, etc., none actually suggesting a Chemung fauna. In this region,
however, we are approaching the vanishing western edges of the Oneonta
formation. At Greene the evidence is very clear that the Oneonta forma-
tion is directly followed by the introduction of a Chemung fauna, and hence
occupies the position which I ascribed to it in my preliminary report, replac-
ing the upper part of the Portage beds and representing, in this region, the
closing stages of Portage time.

Explanation of Geologic Map t.

Tully Limestone.

Previous maps representing the outcrop of this formation have given
only the northern exposures through the central portion of this region. In
the southern towns of Onondaga county, Tully and Fabius, the best known
of these outcrops are in the vicinity of the Tully lakes, and at Tinkers Falls.
The outcrop bends thence southward into the town of Cuyler, Cortland
county, along the eastern branch of the Tioughnioga river, and may be
traced on the west side of the Tioughnioga valley through the town of
Truxton and almost to the township line of Homer. On the east side of this
valley it extends nearly as far to the south-west, bending southeastward for a
short distance up the valley of Cheningo creek, where it is exposed on the
north side, but was not observed on the south side of this valley. An excel-
lent exposure at Station VIP, Tripoli brook, three-quarters of a mile north-
west of Cuyler village, is described more fully in the following pages.

It is seen at several places in the town of DeRuyter, Madison county,
along the south slope of the same valley, passes over the watershed between
that and the Otselic valley, probably extending as far southward on the latter
as the village of Otselic, Chenango county. It is thence continued in the
direction of Smyrna and, as stated by Vanuxem, 8S. G. Williams and Prosser,
disappears by thinning at about one and a half miles northwest of that vil-
lage, in the Chenango valley. At only the station cited does the exposure
give a clear section of the entire formation, measuring about eighteen feet.
The exposures in the town of DeRuyter are of portions of the beds only.

East of Keeney Settlement, near the north line of Cortland county, the
limestone bounds an outlier, extending north into Fabius, east to the Madison

county line, and south to the Tioughnioga.

Genesee Slate.

This formation is exposed at but a few points. It was observed on
Tripoli brook (Station VII*), where about ten feet are shown, and near De-
tuyter (Station I) to a thickness of eight feet, the upper portion probably

being covered. ‘Toward the east it rapidly thins out, disappearing not far
42

i na |!
CTO 7 Tein PO,
oe a Ant
| (

4 NEA

ee

: fe]
t. Z . a :
i ei /
= AE BS Ad
5 | T wall io >
8 zs y S| "aa-b 3
E S . = “he § <
i 2 a ¥ S ' e .
a ALE : ;
ind a o
=< 3

4

AS
7

a TF — =
ee oa
ta w =D ? 4
= e
F Vos ; | = ;
} r YY (Sc
c 5
f as on
Z fr, r
> Be

Mires
alk

ce
Lf 5
\

|
ay

‘e | T ns oe ; wt
ai 3 4 Ce i

ects fe

Rte wy

3 fm Or L

co hee x a i
a 2

ini D ta

Oe

GEOLOGICAL MAp
~ _—_OF A PART OF
Crrenanco AND CORTLAND
ae COUNTIES ~~
z == BY

J. M.C LARKE
1695.

f

iN

—-

CLARKE—OneEontTA, ITHaca AND PortaGE Groups. 43

west of the village of Smyrna, though, as determined by Prosser, it can be
traced somewhat eastward beyond the vanishing point of the Tully limestone.

Sherburne Sandstones.

In adopting this term of Vanuxem’s, I follow the suggestion of Pro-
fessor Prosser, who points out the fact that these beds of sandstones, flags
and sandy shales are continuous from the Chenango river westward at least
as far as the meridian of Cayuga lake. Their lithologic character together
with their notable paucity of fossils permits the identification of them still
farther westward. The heavier beds, lying at the base of the Portage series
in Seneca and Yates counties, indicate an extension of this division into more
westerly regions; but with the growing predominance of the typical Portage
or Naples fauna over that of the Ithaca group, the individual character of
the deposits here becomes gradually lost. In the region, however, between
the Tioughnioga and Chenango rivers, it is a well-defined formation, standing
in sharp contrast to the Tully and Genesee beds beneath and to the beds
immediately overlying, which contain the reappearing and modified fauna of

the Hamilton group.
Ithaca Group (lower division).

The rocks which are properly included within the Ithaca group of
Vanuxem are here represented in two colors, as there is, for this region
at least, a ready distinction in the faunas of the lower and upper beds.
From the detailed description of the sections of these strata given in the
following pages it is seen that the lower division, which is on the whole less
arenaceous than the upper, contains strongly developed faunal characters of
the Hamilton group, a fact clearly brought out by the observations of both
Professor Prosser and the writer at North Norwich, Norwich, South Otselic
and Pitcher Springs, in Chenango county.

Thus at Stations A and B, of my preliminary paper, in the east-west
section from Norwich toward Preston, are such characterizing species as
Phacops rana, Homalonotus DeKayi, Bellerophon patulus, Athyris spiri-
feroides, and Spirifer audaculus, m addition to which are many other species
of the Hamilton fauna which extend into the higher beds of the Ithaca forma-
tion. At South Otselic (Station III), these beds are admirably exposed.
Directly overlying the fucoidal layers of the Sherburne sandstones are compact

dark shales with a small association of certain Hamilton species not abundantly

44 Report oF THE STaTE GEOLOGIST.

represented in the Ithaca beds elsewhere: Hyolithes aclis, Strophalosia
truncata, Pholidops Hamiltonie, Lingula ligea, var. (Hall), and some others.
Above these beds comes in a more extensive and pronounced Hamilton fauna
containing Phacops rana, Spirifer mucronatus (the Hamilton type of the
species), Spirifer asper, Atrypa reticularis (large and finely pleated), Rhipid-
omella Vanuxemi, Actinopteria Boydi (strictly the Hamilton form), and some
others of wider range into the higher beds of the group. While we may speak
of these associations of fossils as recurrent appearances of the Hamilton fauna,
this is not an accurate expression, for there appear associated with such
species as the above, others which serve to demonstrate that this fauna lying
above the lower Portage beds (Sherburne sandstones) is a Hamilton fauna
modified by the introduction of certain species and variations foreign to the
normal fauna of the Hamilton group. One of the most striking witnesses of
this modification is the presence of Leptaena rhomboidalis, found at Station IIT;
of a large and abundant new species of Cyrtina ; of Poteriocrinus gregarius,
Actinopteria zeta and A. perstrialis. The association of species 1s constantly
varying through the different horizons of these rocks; some of them are
restricted in their range, e.g. Phacops rana, Homalonotus DeKayi, Spirifer
asper, and the fossiliferous horizons were generally widely separated by inter-
vals of barren rocks. It is noteworthy that the species Phacops rana and its
associates, which evidence strong Hamilton characters, are less abundant
and much more sharply restricted in the Otselic valley sections where the
whole series is separated from the true Hamilton beds below by the Genesee
shale and Tully limestone, than in the Chenango valley, as at North Norwich
and Norwich, where those beds have totally disappeared from the section.

Ithaca Group (upper division).

The distinctive difference in the lower and upper faunas of the Ithaca
group is due to the introduction of Spirifer mesastrialis. So far as my own
observations extend, and I believe they are confirmed by those of Professor
Prosser, this species does not appear in the lower beds. Its first appearance
at South Otselic was found by Prosser at 585 feet above the valley, which is
essentially the same distance above the top of the Sherburne sandstones. Its
associated fossils have more or less strongly developed Hamilton characters as
shown by the species recorded from sections in the village of Cincinnatus,
Cortland county (Station V, 1894); near Pitcher, Chenango county (Station
T); at Solon, (Station VIII); in the vicinity of MceGrawville (Station IX’);

CrarKE—Owneonta,-ITHAcA AND Portage Groups. 45

north of Marathon (Station XI); and near Lisle, Broome county (Station
XIT).

In their upper portion these beds become distinctly more arenaceous, the
fossiliferous horizons more widely separated. The difficulty of making a
well-defined line of distinction between these upper beds and the formations
of the Chemung group has already been mentioned. So far south as the
formations have been traced by me in the Tioughnioga valley, no satisfactory
evidence of a Chemung fauna has been observed. The fauna found at Lisle
indicates the presence of the Ithaca fauna, and my observations have not
extended south of this point. Professor Prosser reports Dictyophyton and
other Chemung fossils at Whitney’s Point, three miles below.

Oneonta Group.

The attempt has been made to represent upon the map the relation of
this group to the Ithaca group as explained in the introductory pages of this
paper. On the Chenango river the red and green shales and sands rest upon
beds which rarely contain Spirifer mesastrialis. Westward these beds
disappear by thinning, dovetailed into the edges of the upper Ithaca beds,
and at Greene we doubtless have actual superposition of a Chemung fauna

upon the Oneonta beds.

,

The Historical and Actual Significance of the Terms,
“Tthaca Group” and “Ithaca Fauna.”

It is quite essential to acquire a clear conception of the precise footing
upon which the terms Jthaca group and Ithaca fauna now rest in the New
York nomenclature, in order to fully apprehend the difficulties of applying
either in the region eastward of the Ithaca meridian.

The name /thaca group was first used by Professor James Hall (1839).
In discussing the geologic formations of Tompkins and Chemung counties, in
the Third Annual Report of the Fourth Geological District (pp. 318-322),
the account given of this formation and its distribution is so full that I

reproduce it here in its entirety.

““The Ithaca group follows the rocks last described [the shales and flags immediately overlying
the Genesee slate]. Like the preceding, it consists of alternations of shale, both slaty and compact,
and argillaceous sandstone, but differs from it in the contained fossils, and in some particulars of its
lithological character. It sometimes contains thin layers of impure limestone, the calcareous matter
arising principally from the contained shells. This group is well characterized in Ithaca at the inclined
plane of the railroad; it extends also much above the rocks here visible, attaining a much greater
thickness, as can be seen in the valley of the Chemung, south of Seneca lake. In the rocks of this
series individuals of two species of ferns have been found, precursors of the great abundance of that
tribe in the coal formation; and among the many testaceous fossils are Producta, Leptena, Orthis,
Pterinea, etc. These diminish farther west, a few only of the more characteristic occurring on Seneca
lake.

‘‘With the deposition of the Tully limestone the family of trilobites ceased to exist, yet we find
with the characteristic fossils of this group the buckler of Diplewra Dekayi and Calymene bufo, with
other fossils which lived at the period of the deposition of the Moscow and Ludlowville shales.
These fragments, being the lighter part of the animal, were floated upwards with the detritus of the
lower rocks and deposited at this era. Similar instances occur in some of the lower rocks, but the
occurrence of such fossils is not to be considered as characteristic of a rock, or as evidence of their
existence at the time of its deposition.

‘“ At Hector Falls, and above, we find about four hundred feet of this group exposed; the lower
part contains the ferns of Ithaca, and above some of the other fossils. At this place we find a few
thick layers of sandstone, very compact and firm, which have been quarried by Mr. Lawrence. Few
durable building stones are found in this county, if we except this sandstone, which, however, is little
used. It furnishes the fine flagstones used in Ithaca and elsewhere. In general characters it differs but
little from that of the group below, but Fucoides are found in greater quantities on the surface, many
stems of which attain a diameter of two or three inches. One species, the most abundant, occurs on
the under side of the layers, as if growing on the bottom of mud and clay, when overwhelmed with the
inundation of sand. This species is always straight or anastomosing at various angles, sometimes pre-
senting imperfect reticulations, and at other times a fancied resemblance to a bird’s foot. It occurs on
many layers through a considerable extent, though separated by thick masses of shale. The surface of
most of the layers is smooth, or even glazed with a thin coating of shale, which appears to have flowed
over it, leaving marks of unequal deposition and little ridges or prominences where the paste was less
fluid. The deposition of these shales and sandstones progressed slowly, considerable time having
e‘apsed between the deposition of the different layers, and in some instances a lower stratum became
partially indurated before the succeeding deposit was made. There are numerous proofs of the general
operation, and in particular of the latter, where we find, near Jefferson, the surface of a layer worn

smooth and grooved, asif by a current, transporting some hard body over it. The scratches do not
46

CLARKE—Ownronta, IrHaca anp Portage Groups. 47

present the roughness of alluvial scratches, but appear to have been made before the rock was entirely
indurated, or else they have been modified by the deposition of shale which succeeded. In this instance
I have not been able to ascertain the direction of the current, though it was probably from the north,
and like all other currents in the ancient seas, took the direction from the greatest elevation to the
lowest point.

“Tn some localities the sandstone is replaced by a kind of sandy shale, being a mixture of sand
and clay, and the whole is rippled, the markings affecting each thin layer, and showing that it was
deposited from water in motion, which might transport from different directions the two materials of
the rock. This group appears to have been deposited from an ocean alternately at rest and disturbed,
Thick masses of sandy shale occur, bearing ripple marks through their whole depth; these are succeeded
by others of variable thickness, without ripple marks, and having the faces smooth and -plain.
Numerous alternations of this kind have been noticed through many hundred feet. Fossils never
accompany the rippled layers, but are invariably found with the smooth. The materials of the two
differ very slightly in mineral composition, the rippled ones being more sandy. The absence of fossils
in the latter may be explained by supposing the unquiet state of water during the deposition of the
rippled shale to have been unfavorable to the development of organic life. So far as I have observed
in this and other localities, the greater accumulation of fossils is always accompanied by fewer ripple
marks.

‘‘The changeful state of our planet at that period may have occasioned numerous risings and
sinkings of the crust, some portions of which may have been disturbed oftener than others, one under-
going the oscillatory movement while another was at rest. This may be considered proved from the
fact that undulations are exhibited in some localities, while a distance of a few miles shows a plane and
undisturbed surface. Thus the undulations of the rocks on Seneca lake have not been communicated
to those on the western shore of Crooked lake, although the latter are part of the same mass, separated
only by a distance of ten or twelve miles. The valley of Crooked lake could have had no influence in
interrupting the motive force, as probably at that time it was not excavated; and farther south we find
other undulations of which the counterparts are exhibited on each side of the valley.

‘These uplifting movements would form bays or protect some portions of the sea where animals
might exist in great numbers, while every other part for miles in extent were too unquiet for the
development or preservation of animal life.

“Tn numerous localities of these rocks the edges of strata, when exposed in ravines and other
places, are found covered with crystals of sulphate of lime. This circumstance is by no means universal
among the shales below, although observed in some localities, while in the present group there are few
exceptions. Pyrites in minute particles are everywhere disseminated, decomposing on exposure and
hastening the destruction of the rocks, while the sulphuric acid combines with the minute proportion
of lime which they contain, exhibiting the crystals along the edges. Wherever larger masses of pyrites
occur we find a proportionate increase in the quantity of sulphate of lime. Similar conditions in some
of the limestones below have produced a mass of gypsum, filing the cavity previously occupied by the
pyrites; and analogous circumstances, varying in extent and effect, may have formed the vasc
gypsum beds of the same series, extending throughout the whole of western New York. The latter,
however, could only have occurred before the entire induration of the surrounding rocks.

“CHEMUNG COUNTY.

“In this county the group last described forms the surface rocks of the northern towns, and in the
ravines and valleys extends south to the southern line of the towns of Veteran and Catlin. The rocks
here retain most of their essential characteristics, but fossil shells are exceedingly rare, and in many
localities entirely wanting. The peculiar fucoidal markings are everywhere preserved in the thin layers
of sandstone. The rocks of this group are well developed in Gulf creek, near Jefferson, at the head of
Seneca lake, and at many points south on the west branch of the valley and the ravines coming into it.

‘‘ From Jefferson to Millport the rocks dip south, exhibiting throughout continued alternations of
shale and sandstone, and towards the upper part the compact shale is covered with fragments of a
Fucoid, different from those below, and appearing only in curved fragments.

‘¢Tn the vicinity of Millport and farther south the sandstone layers attain a thickness of a foot or
more, and are quarried for works on the canal and various other purposes, and at Pine valley the sandy
layers of the rocks are quarried in two places. Mr. Sexton, the owner of the last, informs me that the

48 Report’ OF THE STATE GEOLOGIST.

firmest layers of sandstone often pass into shale so as to be unfit for any economical purpose. This
appears to be unlike the thinning out of the layer, but the proportion of argillaceous matter becomes so
great that the mass crumbles on exposure.

‘*At the last-named quarry I observed the singular fact of non-conformable strata, as yet the only
instance noticed, and which various circumstances seem to render incredible. The strata are parts of
the same mass, Once continuous, the lower dipping south at an angle of four or five degrees, and the
upper dipping north at about the same angle; and a short distance farther south the whole mass dips
north. The only explanation that now offers is that at the time the rocks were subjected to the force
which produced the undulations the upper part slipped over the lower, and at this point partook of the
elevation south, while the lower was affected only by the uplifting to the north. The point of the
greatest depression is a short distance south of this locality. In this quarry was found the only speci-
men yet seen of a fern of the genus Sphenopteris, and through the liberality of Mr. Sexton, to whom I
am farther indebted, I am enabled to place this specimen in the collection of the State. With the
exception of the curved fragments of Fucoides, the upper part of this group is nearly destitute of
fossils.”

This description of vertical extent of the Jthaca group, though not giving
a definite conception of its lower limit, specifically carries its upper limit so
far south as to include the heavier sandstone beds at Millport and further
south. Our evidence now points to the fact that these sandstones are contin-
uous with the typical Portage sandstones of the Genesee valley. The expo-
sures near Millport are of these sandstones; Jefferson is the former name of
the village of Watkins, and the rock section there is essentially reproduced
in the Havana glen section given in detail in the following pages. All this
region of country, then a part,of Chemung county, now constitutes a part of
the county of Schuyler.

The historical J/thaca group is thus the sedimental equal of the major
part of the entire Portage formation. Professor Hall’s description, while
showing the lithologic similarity of the /thaca group to those beds along
the Genesee river to which he subsequently apphed the names Cashaqua
shales, Gardeau flags and Portage sandstones, also suggests a critical difference
in fossil contents though without citing such data as can serve the require-
meuts of the present day.

In subsequent reports of geologists Hall and Vanuxem, the Jthaca group
was not similarly construed. Vanuxem, in his Fourth Annual Report (1840),
p. 381, places the Jthaca group between the “Sherburne Flagstone” and the
“Chemung group,” saying: “Consisting of sandstone and shales, forming a
thick mass, highly fossiliferous. Names not [yet] given to the fossils. The
top part of this mass terminates in a series of these sandstone flags with
fucoides resembling those below the group, and which separates the succeed-
ing group from the Ithaca.” This view accords with the original definition
of the term.

In his report for the same year Professor Hall made no further reference
to the Ithaca group except to include it in tabulations of the New York for-

CrhaRKE—OneEonta, -IrHaca anp Portage Groups. 49

mations given on pp. 452, 458. On the former it is placed between the
“Cashaqua shale” and the “Gardeau and Portage groups ;” on the latter it is
given the same stratigraphic position, between the “Cashaqua Shale and
Sandstone” and the “ Gardeau Flagstones.”

In Vanuxem’s final report on the Third District (1842), the /thaca group
is placed in the succession above the “ Portage or Nunda group,” (pp. 12, 18,
174). It is perfectly evident, however, from reading the accounts of both of
these groups, that Vanuxem had no clear conception of the true relations of the
formations and was accepting the last named division on the evidence derived
from the Fourth District. His description of the /thacu group is quite brief
and, in the special discussions by counties, the Portage and Ithaca groups are
generally mentioned together without further attempt at distinction, the
former division being represented by the rocks which this author had origi-
nally termed the “Sherburne Flagstones.” Then, as to-day, there were no
difficulties in apprehending the value of this “Ithaca group,” eastward of the
Ithaca meridian.

The final report on the Fourth District (1843) places a new construction
on the formation. On page 250, Professor Hall remarked :

“Tthaca group. In the annual reports this name was adopted for desig-
nating the highly fossiliferous shales and shaly sandstones, so well developed
at the inclined plane of the railroad and on the Cascadilla and Fall creeks
near Ithaca. Subsequently an examination of the highly fossiliferous strata
along the Chemung river, and particularly in Chemung county, resulted in the
adoption of that name as designating this portion of the system.

“Succeeding examinations satisfied me of the identity of the formations
at Ithaca with those of Chemung, and this opinion was advanced in the
annual report of 1841.

“The reasons for merging the two in one were stated.to be the impossi-
bility of identifying them as distinct by any characteristic fossils. The same
opinion is stil] entertained after a full examination of the strata, and a com-
parison of the fossils collected here and elsewhere in well authenticated
localities of the Chemung. ‘There is scarcely a fossil known at Ithaca which
is not found at numerous other localities; though it is true not only of Ithaca
but of many other places that some of the fossils are confined to a single
locality in which they occur.”

Largely in consequence of this opinion, the term thereafter passed into

desuetude.
4

50 Report oF THE SvrarE GEOLOGIST.

In the subsequent New York reports the section at Ithaca has been gen-

erally referred to as lower Chemung, doubtless in the broader application of

g,
the name Chemung as a major term for all the upper Devonian sediments of
this meridian. So completely was the name lost sight of, that in volumes of
the Palaeontology of New York, many localities lying within the limits of the
Ithaca group, especially as this term was employed by Vanuxem in the Third
Greological District, were cited generally as of the age of the Hamilton shales,

though sometimes referred to the Chemung; and in Dana’s “Manual of

g;
Geology,” 3d edition, 1880, the name /thaca group does not appear.

Up to this date the fauna of this group had received no attention
further than that indicated in the foregoing extracts from Professor Hall’s
reports, and the depiction by Vanuxem of two of its brachiopod species, only
one of which is now recognized, Leptostrophia mucronata. In 1884, Prof.
H.S8. Williams published an account of the succession of the faunas in the typical
section of the /thaca group (Bull. No. 8, U.S.Geol. Surv.). This is an important
document for the reason, among others, that it clearly shows the presence here
in repeated manifestations of two distinct faunas, the one from the west,
marked by the presence of gomiatites and cardioconchs, and by the absence of
brachiopods ; the other from the east characterized especially by the prevalence
of Hamilton types of brachiopods and lamellibranchs ; the former is the fauna of
the typical Portage series of the western sections, the latter is termed by Williams
the Jthaca fauna. This is the first precise use of this expression, and it is at
once clearly evident that this Ithaca fauna is not the fauna of the /thaca group,
as outlined by Hall, but of only a part of that group. The section studied
by Willams shows that here the fundamentally distinct faunas of the east
and west are interleaved and commingled, each encroaching upon the province
of the other and, in turn, bemg invaded by that other, so that in a vertical
section the succession presents the aspect of rapid alternations of these faunas.
The data given by Williams permit the construction of the accompanying
diagram (Figure 5) designed to express the interpenetration of the two faunas
along this meridian, it being understood that the interlocking angles are
highly exaggerated. The author has distinguished several subdivisions of the
eastward fauna but restricts the term “Ithaca fauna” proper, to its uppermost
or latest manifestation. The fundamental distinction in the eastern and west-
ern faunas is, however, sharply defined from bottom to top, and the eastern
fauna, manifesting itself near the base of the series in the Cladochon us faund,
ends only with the disappearance of the “Ithaca fauna,” 500 or 600 feet below

the first appearance of well defined Chemung species. The “recurrent Hamil-

CLARKE—ONEontTA, -lrHACA AND PorraGE Groups. bil

ton fauna” lying not far below the “ Ithaca fauna” (as restricted by Williams),
is such a reappearance of strong Hamilton types as we have observed in even
greater force at a lower horizon in the rocks both at South Otselic and at
Norwich, and is not in any sense out of harmony with the rest of the fauna

which is, in the main, a similar recurrence of Hamilton types. Williams’s

CHEMUNG

Prerochaens

Buchiola

Spiriter laevis

Modtomorpha

Microdon :

Atrypa Grammysia
Actino pteria Brallecs h

Orthis pion.

Stropheodonta
Chonetes ITHACA FAUNA Proper

Productelle

Tornoceras

Rhynchonella PleuroTomaria
Cyurlhina

Spirvfer mesacostalis

) Orthoceras Arthracantha

Tornoceras

ikl mesastnalis
Microdon Atrypa. Rhynchonella \STatro N 5) a “ye enella c
qrtmna

W Shiclopera

Poterioctinus (STATION 37) peas Ser
Rhynchonella 4tTina

Spirifer Ambocoelia,tlothynchus

RECURRENT HAMILTON
Rhynchonella —= =

Microdon Modiomorpha

Nhunchenelia:/ S tation 4)

Buchiola
Microdon hithamvc Productella
‘Probeloceras
Bactrites Buchiola Leda Tax octinus
Gramm sia
Chonetes Cyrtina 4
Liorhynchus SPiRIFER LAEVIS Fauna
| Manticoceras Modiomorph
Tornoceras ss ’ Sticto
Probeloceras ee
Bactrifes
Buchiola : C=
ammysia
S n N uculites
Chonetes, piriter, LADOCHONU«S fauna
JLADOCHONUS

Manticoceras,

Liovhynchus,
Pinnopsis,

Chaenocardiola,

Stropheoel
Buchiola, “Bactrites pheoclonta

GENESEE SLATE

FIGURE 5.

| “Ithaca fauna ” is that part of the more easterly fauna which comes in above the
horizon of Spiriter mesastrialis, a division which is of local significance as, in
the counties to the east, Cortland and Chenango, Spirifer mesastrialis haying
once appeared, manifests itself throughout all higher beds of the formation.
A comparison of the succession at Ithaca with the results we have obtained

in Chenango and Cortland counties indicates a general equivalence exemplified,

52 REporT OF THE STATE GEOLOGIST.

for example, in the presence of the Cladochonus fauna at various points, the
appearance of Spirifer levis at Station IX", and its second and final appear-
ance at Cowles hill, Greene, strong reappearances of Hamilton types, as citea
above, and the relative position of Spir7fer mesastrialis in its first appearance,

While it is doubtless correct, to a certain degree, and in accordance with
the views expressed by Professors Hall and Williams, to regard the entire
fauna present in the strata lying between the Sherburne flags beneath ana
the well defined Chemung fauna above, as a transitional expression from the
Hamilton to the Chemung fauna, it is evident that this fauna requires a
single term, as the expression of its relation to the single geologic horizon to
which it pertains. If, therefore, the term “Ithaca” is to be perpetuated in
geologic nomenclature, it must be modified slightly as a geologic term, and
expanded in tts application to the fauna.

In view of the fact that the local name was unfortunately chosen and that
the typical section is through interpenetrating faunas neither of which is at
its normal, it would probably be advantageous to our nomenclature if we
should follow the example of Professor Hall in abandoning the term in all its
applications; such procedure would bring us at once to a ready solution of
our difficulties, as excellent terms expressive of the formation and the faunas in
their purity are at hand in the counties of Cortland and Chenango. The
Otselic river, rising in Madison county and meeting the Tioughnioga at
Whitney’s Point, transects in an almost north and south line the entire for-
mation in its best development, and affords numerous admirable exposures of
both rocks and faunas, The term, Ofselic group, for the geologic formation,
and its equivalent, Otselic fauna, tower Otsclic fauna for the earlier mani-
festations without Spirifer mesastrialis and with the Hamilton expression
strongly emphasized; the upper Otselic fauna for the later expressions with
Spiriter mesastrialis, would be precise and grateful terms. Eventually such
terms will be required, but with proper respect to historic rights, we, for
the present, continue to employ the old terms though with a modified
meaning,

It is my desire to enforce, at this pot, the far reaching contrast in the
western, or Naples, and the central, or Ithaca fauna of the Portage epoch, but
this is possible only under disadvantages. The Naples fauna is composed to
a very considerable degree of unnamed species, many of which can be men-
tioned only in paraphrase, and no one has yet recorded in full the composition
of the Ithaca fauna. The lists which are appended are compiled from my own

records with the aid of those published by Professors Williams and Prosser.

Oe

CLARKE—OneEonvT<A, -[trHACA AND PortaGE Groups. 58

This cautionary remark seems in point. The occasional occurrence of
species of one fauna in association with those of the other and especially
within the province of’ that other, is not to be construed as conclusive
evidence that the species appertains to both faunas alike. Thus, Wanticoceras
Patersoni is one of the indicial fossils of the western or Naples fauna; it is
occasionally found to have wandered eastward among the species of the
adjoming Ithaca fauna; it is thus in the Ithaca fauna, but not of it. The same
is true of several other species, and in separating the indicial features of these
two faunas, such facts must be carefully considered.

In this list are included the species of the Stylola layer (Genundewah
limestone) of the Genesee slate, which represent, as shown in other places,

the earliest appearance of the Naples fauna.

Partial list of species constituting the Partial list of species of the normal
PORTAGE (Ithaca) FAUNA in PORTAGE (Naples) FAUNA in

Chenango and Cortland counties: Ontario and Livingston counties:

Dinichthys Newberryi, Clarke.
Acanthodes priscus, Clarke.

Palzoniscus devonicus, Clarke.

Rhinocaris (?) Cipennis, Clarke. Conodonts.

Phacops rana, Green (sp.). Echinocaris Whittieldi, Clarke.

Homalonotus DeKayi, Green (sp.). E (2) Beecher, Clarke.

Manticoceras Patersoni, Hall (sp.).* Manticoceras Patersoni Hall (sp.).
Re “yar. styhophilum, noy.
“ var. contractum, nov.

M. simulator, Hall (sp.).
M. nodifer, Clarke.
M. tardum, nov.
M. accelerans, nov.
M. oxy, nov.

Gephyroceras perlatum, Hall (sp.). Gephyroceras Genundewah, nov.
G. ceryceum, nov.
Anabeloceras pseustes, nov.
Beloceras iynx, nov.
Probeloceras Luther, Clarke.

Sandbergeroceras syngonum, nov.

* The names here applied to the cephaiopoda are those employed by the writer in an account of this element of the Portage
fauna, now ready for the press.

54 Report oF THE STATE GEOLOGIST.

Tornoceras uniangulare, Hall (sp.).

Hyolithes achs, Hall.
Tentaculites bellulus, Hall.

T. spiculus, Hall.

T. sp. noy.

Styliolina fissurella, Hall (sp.).
Conularia undulata, Hall.
Bellerophon patulus, Hall.

B. sp. nov.

Platyceras sp.

Murchisonia micula, Hall.

Pleurotomaria sulcomarginata, Conrad
Po ck. ctrilix, all | (sp.).
P. Itys, Hall.

Liopteria levis, Hall.
L. Sayi, Hall.
L. Greeni, Hall.

Tornoceras uniangulare, Hall (sp.).

«s var. obesum, nov.
= var. compressum, Nov.

T. peracutum, Hall (sp.).

T. bicostatum, Hall (sp.).
Cyrtoclymenia Neapolitana, Clarke.
Bactrites cf. gracilis, Sandberger.
B.

Orthoceras pacator, Hall.

O. Ontario, Clarke.

O. filosum, Hall.

Gomphoceras, sp.

Hyohthes Neapolis, Clarke.

Tentaculites gracilistriatus, Hall.

Styholina fissurella, Hall (sp.).

| Clarke.
Bellerophon striatus (Ferussac),
B. natator, Hall.
B. ineisus, Clarke.
Loxonema Noe, Clarke.
Palzeotrochus preecursor, Clarke.
Protocalyptrzea Marshalli, Clarke.

Pleurotomaria Itys, Hall.

P. Itys, var. tenuispira, Hall.
Diaphorostoma minutissimum, Clarke.
Diaphorostoma, sp. nov.
Macrochilus, sp. noy.

Liopteria levis, Hall.

“ Ungulina” suborbicularis, Hall.
Cardiola Wyomingensis, Williams.
C. Varysburgia, Williams.

C. Doris, Hall,

Cardiola, several undescr. species.
Buchiola speciosa, Hall (sp.).

Buchiola, several undescr, species.

——

” ae

CrarkE—Oneronta, IrHaca AND PorraGEe Groups. Di

Ot

Lunulicardium ornatum, Hall.
L. fragile, Hall.
L. leve, Williams.
L. many undescr. species.
Pholadella, sp. nov.
Paleoneilo emarginata, Hall. Palzeoneilo muta, Hall.
P. constricta, Conrad (sp.).
P. brevis, Hall.
P. fecunda, Hall.
P. maxima, Conrad (sp.).
Leda diversa, Hall.
L. brevirostris, Hall.

Paracyclas lirata, Conrad (sp.).

Leptodesma Rogersi, Hall, Leptodesma sp.
Microdon bellistriatus, Hall. Ptychopteria mesastrialis, Williams,

M. gregarius, Hall.

Nucula lirata, Conrad (sp.).

N. corbuliformis, Hall.
Modiomorpha subalata, Conrad (sp.).
M. mytiloides, Conrad (sp.).

M. concentrica, Hall.

M. sp. nov.

Modiella pygmzea, Hall.
Gonlophora rugosa, Conrad (sp.).
G. subrecta, Hall.

G. Hamiltonensis, Hall.
Mytilarca sp.

Grammysia constricta, Hall.

G. magna, Hall.

G. elliptica, Hall.

G. bisulcata, Conrad (sp.).

G. arcuata, Conrad (sp.).
Sphenomya cuneata, Hall.
Cimitaria elongata, Conrad (sp).
Sphenotus contractus, Hall.
Actinopteria Boydi, Conrad (sp.)
A. perstrialis, Hall.

A. zeta, Hall.

56 ~ Report oF THE State GEOLOGIST,

A. eta, Hall.

Schizodus appressus, Conrad (sp.).
Spuifer mucronatus, Conrad (sp,).
% - var. posterus.

levis, Hall.
Tullius, Hall.

. sculptilis, Hall.
mesastrialis, Hall.

Gp)

Tf )

)

Py’

wn wp

asper, Hall.

audaculus, Conrad.

op. }

Cyrtina Hamiltonensis, [all.

C. ef. curvilineata, Hall.

C. sp. nov.

Leptostrophia mucronata, Conrad (sp.)
Strophonella perplana, Conrad (sp.).
Leptena rhomboidalis, Wilckens.

Strophalosia truncata, Hall. Strophalosia truncata, Hall.
Orthothetes arctostriata, Hall (sp.). Orthothetes arctostriata, Hall (sp.).
Productella spimulicosta, Hall.

Chonetes scitula, Hall. Chonetes scitula, Hall.

C. lepida, Hall.

C. deflecta, Conrad (sp.).

Rhipidomella Vanuxemi, Hall (sp.).

Schizophoria impressa, Hall (sp.).

Tropidoleptus carinatus, Conrad (sp.).

Atrypa reticularis, Linné.

Liorhynchus mesacostalis, Hall.

Amboccelia umbonata, Conrad (sp.).

Athyris spiriferoides, Eaton (sp.).

Camarotcechia congregata, Hall (sp.).

Pholidops Hamultonize, Hall.

Lingula ligea, var. Hall. Lingula ligea, var. Hall.
L. triquetra, Clarke.
L. spatulata, Hall.

Stictopora Gilberti, Meek.
Aulopora annectens, Clarke. Aulopora annectens, Clarke.
Cladochonus. Cladochonus.

t

~
=~I

CrarKE—Oneronrs, [ruaca AND PortraGre Groups.

Melocrinus tricyclus, Eaton (sp.). Melocrinus Clarkei, Williams
Poteriocrinus gregarius; Williams.

Taxocrinus Ithacensis, Williams.

Without further comment, the fundamental difference in these two
faunas is apparent, the one (Ithaca) indigenous, whose ancestral stock mani-
fests itself in the immediately preceding faunas; the other exotic and
introduced, The latter characterized by its high development of the Goniati-
tine, of Lunulicardium and the cardioconchs, the former by their absence.
In fact, there is almost nothing common to the two faunas in their purity,
and it is fair to infer that, as suggested above, the few Ithacan species present

in the Naples beds, have strayed in from the east.*
The Seneca Lake Section.

The reader who cares to follow the detailed description of sections in
Schuyler and Yates counties given in the following pages will see nothing
more clearly than the westward disappearance of the Ithaca element in the
composite fauna of these meridians.

This lessening of the eastern elements makes itself manifest in the lone
section made at Havana (Stations XII and XIV). The rocks of this region
are very sparsely fossiliferous and the various substations listed in Havana Glen
indicate each a separate association where species of the two faunas are often
present. In following the general trend of the formation to the northwest,
into Yates county, a distinct increase im representatives of the Naples fauna is

* Since this report was written I have received, by the courtesy of Professor G. D. Harris, of Cornell University, a copy of No
6, of his “‘ Bulletins of American Palaeontology,’ dated December 25th, 1896, and entitled: The Relation of the Fauna of the
Ithaca group to the Faunas of the Portage and Chemung (pp. 1-56, plate 1), by E. M. Kindle.

This useful contribution gives a review of the succession of faunules in the Ithaca section and adds considerably to the known
lists of species and local manifestations of the faunules.

These lists show that, with the alterations in appearance of the eastern and western faunas, there not unfrequently occurs
an actual commingling of the species of the two at one plane. They serve also to enforce the importance of the cautionary
remarks made above, that an elucidation of the true nature of the faunal constitution in this rock series is not possible without
a clear comprehension of the two distinct faunal elements entering into its composition.

It seems necessary for me to advert here to a single point raised by Mr. Kindle as to the propriety of the term Naples beds,
which I introduced in 1885 for the strata which bear the Intumescens fauna. It is observed that Professor H.S. Williams, in
describing the lower Chemung fauna at High Point, in the town of Naples (American Journal of Science, vol. xxv, p. 97, 1883), a
fauna which appears at several hundred feet above the first clear manifestation of the Chemung fauna in that meridian, applied to the
containing strata the term Naples beds, and that, hence, this term being of totally different significance from my use of it, its earlier
date entitles it to precedence. I have to confess that this is the first time my attention has been directed to the employment of
this term by Professor Williams. Upon turning to his paper ‘‘On a remarkable Fauna at the base of the Chemung group in New
York"’ (doc. cit.), I find this expression used but once and in the following language: ** The author is indebted to the kindness of
Professor J. M. Clarke, of Northampton, Mass., and Mr. D. D, Luther, of Naples, N. Y., for the discovery of these Naples beds”
(p. 97). This is, as Professor Williams himself would doubtless admit, but a casual expression, one of several used in the same
paper to express a similar meaning, thus: ‘‘ The Naples rocks”? (p. 97), ‘‘the High Point fauna”’ (p. 97), “the fauna at High
Point” (p. 99), ‘‘ High Point beds” (p. 99). These expressions are each used several times, while ‘‘ Naples beds’”’ occurs but
once in the paper and has never been employed since by Professor Williams or any one else with reference to the now wel!-
known High Point fauna of the High Point beds, which are, with these terms, qnite sufficiently denominated. The term “ Naples
beds”’ has come into use, with well defined meaning, as a local name for the strata which carry the fauna of the Intumescens-zone,
and the term has been neither conceived nor employed as a geologic designation in any other sense.

58 Report oF THE STATE (ZEOLOGIST.

evident. This is seen in lists from stations along the west shore of Seneca
lake (XV, XV!, XV?, XVI, XVII). At Belknap’s Gully, two miles north of
Branchport, Yates county, the fauna has, so far as observed, virtually lost
its Ithacan component and presents only species abounding in the Naples
section. ;

Now and then among the fossils in the Ontario and Livingston county
sections will be found a straggler from the east; Ovrthothetes arctostriata,
Liopteria laevis and Strophalosia truncata are among the less frequent forms.
The pelagic Stylolina fissurella has been swept in in enormous quantities.
Chonetes scitula and Ambocelia umbonata are occasionally seen. With the
exception of Sty/iolina, these are all of unusual occurrence, and we have
evidence that such isolated representatives of the Ithaca fauna are to be
found in the Naples fauna as far westward as Erie county.

The boundary lines of the Portage series of rocks have been, by the
labors of Mr. D. D. Luther and the writer, made out with precision in
Ontario and the adjoiing counties. In the Naples section the vertical thick-
ness of these rocks from the Genesee shales to top of the Portage sandstones
is 600 feet. These heavy-bedded Portage sandstones were regarded as the
upper boundary of the Portage series in the original delimitation of the
group, and they form a well defined bench mark throughout western New
York, but in more westerly sections they are overlaid by a considerable mass
of flags and sands which continue to carry a Naples fauna with some modifi-
cations, but embracing no typical Chemung species.

The faunules of the beds lying immediately below the heavy sandstones
are, in interesting respects, unlike those of the more prolific beds below. Thus
in Naples village, at a distance of twenty feet below these beds, are shales
with a Naples faunule, viz.: Buchiola speciosa, Bactrites, Palwoneilo muta,
Cardiola sp. Pleurotomaria capillaria, Manticoceras Paterson’. Just below
the heavy-bedded sandstones comes in a faunule unlike anything observed
beneath, im this section; abundant in individuals though not in species, viz. :
Liorhynchus, which at maturity is of large size and has the aspect of Z.
quadricostatus, while younger shells resemble Z. /imitaris of the Marcellus
shales; Atrypa reticularis of small size with coarse plications, and three or
four strong concentric varices, free at their edges; Pvoductella speciosa, Lep-
tostrophia mucronata and an Orbiculoidea, probably undescribed, Evidently
this faunule has entered from the east, and it heralds the dispossession of the
Naples fauna and the occupancy of the region by wholly distinct types

of life.

CLARKE—OnkeEonTA, ITHACA AND PorraGE Groups. 59

Recent observations, on this meridian, have shown, and undoubtedly
future investigations will give us much more detailed evidence of the fact
that about these Portage sandstones, for a few feet above and below them, are
repeated oscillations of faunules, some of them with Naples species, others
with forms of later date.

At the village reservoir, Naples, just beneath the sandstones and hence
at the horizon of the faunule above mentioned, occurs a species of Leptodesima
of distinctly Chemung aspect, though undescribed. Again, Mr. Luther has
recently found at the base of these sandstones in the Tannery gully several
interesting species of Dictyosponges. In the same section at about 100 feet
above the top of the Portage sandstones comes in a well defined Chemung
fauna, shown at Deyo basin with [ydnoceras tuberosum, Ceratodictya annu-
lata, Hydriodictya, Ambocalia umbonata var. gregaria, Spirifer mesacostalis,
Atrypa hystrix, Productella speciosa, Arthracantha ; on the West Hollow road,
near Charles Sutton’s, with Orthis Tioga, Liorhynchus mesacostalis, Produc:
tella spinulicosta, Ambocelia umbonata; and at the Hamlin farm, with
Hydnoceras tuberosum, Aviculopecten cancellatus, Sphenotus sp. Ambocelia
umbonata, var. gregaria, Stropheodonta Cayuta, S. variabilis, S. arcuata,

Leptostrophia perplana var. nervosa, Arthracantha.

Explanation of Geologic Map 2.

The purpose of this map is to express graphically the gradual change
westward of the fauna of the Portage rocks.

At the eastern limit of the region the fauna is the commingled Ithaca
and Naples faunas; westward the former element is lost and the typical
Naples species gradually attain predominance.

60

page>> 0% TE ee =>. ae wa” Tn 1S
: A] pre pCakbetos Pia x 3

3 —TT peer —

Cy | Age ft

A.
i}
Te

his
AN

i
ly en
AEC

GEOLOGICAL m,,,
SHOWING THE DISTRIBUTION —
=—— oF THE PORTAGE ROup \)
SENECA SCHUYLER YATES —
AND PARTS OF
TOMPKINS a ONTARIO COUNTIES
J.M.CLARKE 1895

a NORMAL ITHACA FAUNA EASTWARD OF THIS REGION

fed ip :

| COMMINGLED [THACA & PORTAGE FAUNA

fail IVE
he orn f s a 7 { |
— es FS ee
| | Normal PORTAGE FAUNA. \| J Or ria
: L7PTEAAN SL

y

iff
)

LAT tnd Y

Summary.
(1) The fauna of the Ithaca group is a modified Hamilton fauna; it

contains a more abundant representation of unmodified Hamilton species in
the meridional section along the Chenango river where the Tully limestone
and Genesee slate are absent. The Hamilton features of the fauna are most
strongly expressed in the lower part of the group, before the appearance of
Spirifer mesastrialis, The fauna of the rock section at Ithaca is not normal
and typical but contains an intermingling of Ithaca and typical Portage
(Naples) species. The terms /thaca group and Ithaca fauna are inexact, and
their continued employment is at the cost of precision and lucidity.

(2) The Oneonta group, comprising sandstones and shales often highly
colored with red and green, occupies the upper part of the Portage series as
developed along the Chenango valley and eastward. West of this valley these
beds rapidly disappear, thinning out and penetrating the upper beds of the
Ithaca group and being penetrated by them. Above them le proemial
Chemung faunules.

(3) Westward of Cortland county the Ithaca fauna gradually becomes
almost totally extinct and is as gradually replaced by the fauna of the typical
Portage series (Naples fauna).

(4) Above the Portage sandstones which cap the typical Portage sec-
tions west of the Naples meridian, are indications of the final appearance of
the Naples fauna through a considerable thickness of strata.

(5) In the Canandaigua lake section the Portage rocks have, probably,
not more than one-half the thickness exhibited in the sections through
Cortland and Chenango counties.

(6) The Portage group is a series of arenaceous deposits representing the
geological time which elapsed from the close of the Hamilton period (includ-
ing the Tully limestone and a portion of the Genesee slate, where present)
to the opening of the Chemung period. The typical and unmixed fauna of
its westerly sections has little organic relation to the proper fauna of the
Hamilton shales, the Chemung fauna succeeding, or the Ithaca faunas
adjoining on the east. It is an exotic fauna, evidently derived from the
west, and making its first appearance in the Genundewah limestone of the
Genesee slates. It is the Vaples fauna.

The fauna of the central and east-central sections is an indigenous fauna,

and its organic composition stands in the closest relation to the fauna of the
61

62 Report oF THE Stare GEOLOGIST.

Hamilton group, but in its later manifestations assumes many characters of

the Chemung fauna. In the Chenango valley and eastward the upper portion

D
PORTAGE GROUP re)
= Q “:
o> = S é
ou = 2z be
ze ~ <u. | ;
<- oS z <
z< L we 2
w 5 —— =
: 2 Fe | lee
s — ~
=) =
“ ee
z
nD \-o
S f
E Pkg
3 } EV
it fa
Be > V
a) 2 |. |
Z = A 2
é wie s 9 a
2 hig = oe z |} =)
2 | = < ©
=
3 30h e = “ oo
fad ‘ = s < # =
4 a )
° <i = ° Zz a a
v 3 = oO - } S
é : = z o ae
r ; xy) u om
eer) = Hh 5D & °
ES 3 2 =j | < "
bs ie = ohe =| 5 { 2
f. < > o oO
Resa ae fg eS < | $
a. <et Sigh bs pA x . =
+ > > > ~ =z } =
tou en jy S) - f =
ete <:2 | = 5
} 2 2° =oa bi? a i s
See yr- Sere . 2s =)
pets: § 23 gh) 8 | 2
- < =
\ zi BS lo
Ng =e |} us a
He) Sa < 4) 2
Se “ S
Pr S| < ai 3
< > 2s = wizl «=
= | Aa ne = alu 2°
= or O as = <| a
2 yet = of =x ~
i ial | = ft
HI] Ss 71 Ss
> > us) —
Kb ot el >
pu, TEE. 4 oe =
sla o+ z)- D
Byt So uw
mi Ss s/2] 8
il) | =r faa i< —
Hi Z 5 = ~~
es ‘= 2
: at 3 j <=
o sh O 2
G:=3 = 5
eae | <i 3
< feist} =) 2 =
= eee, ts 2 =|
=" . o @ a -
I v < —
=~ ;
< S f ao = a
z ” eal %
a) =| =
Sowa B ~
< — Ss
x ug an) a
%
< ” —
a ot 5 B
Se Piel ~ =
ee AS &
a dy “And a
<o. = @
= a | +
ce .
ta <a, ES
ei = Mel Fil 4
+
Feet ry ss)
fa 8 | a
a: So. - er “3 3
& S32 ta
Reese, rY +
E “3 1 2
sO 2 A 3
cL = we
> a =
P55
~> = '
sige! ma x:
E- es | : as
2$ 2 I ws
uw” Gis a z<
vy $ = w”
———— 6 =
dNOYD 3JDVL4O"d “3

of the deposits of this age is represented by the Oneonta group with a very
sparse fauna and well characterized strata. In Chenango county they

replace the higher beds bearing the Ithaca fauna.

Description of Sections in Chenango, Cortland, Schuyler
and Yates Counties.*

Station I.+ De Ruyter, Madison county. A small ravine on the farm of
Mrs. Pamela Burdick, one mile south-east of the village and just east of the
road leading due south to Burdick settlement, shows an exposure of Tully
limestone, eighty-six feet above the creek level at the bridge (DeRuyter).
The exposure of this rock is seven feet and the outcrop is compact and. thick-
bedded, the thin beds which in this vicinity usually compose the lower por-
tion of the formation not being shown.

Overlying, with exposed contact, are the black Genesee slates, eight feet
thick, possibly covered for a few feet at the top. These shales are arenaceous,
scarcely bituminous, non-fossiliferous, without concretions or evidence of the
Styliola limestone.

Above are characteristic Portage sandy shales and sands in thin layers,
with “ Fucoides graphice,” and other inorganic markings, especially a crus-
tacean trail which characterizes the horizon through all the more westerly
sections. Awlopora annectens, Clarke, is the only fossil observed.

Among these sands are intercalated thin layers of olive green, homo-
geneous, smooth sandy shales, without fossils. ‘These rocks continue to the
top of the ravine, which opens on a cross-road. Thickness from base of Tully
limestone, as exposed, to road, 180 feet.

On the upper (south) side of this cross-road is an old quarry (the Burdick
quarry of Vanuxem’s final report) from which stone was taken for the old
DeRuyter Academy, Near the lower part of this exposure the elevation is
forty-five feet above the road. The rock here exposed is much softer and
more argillaceous than that below, less arenaceous and more-slabby.

This hill-side also bears a smaller, shghtly worked exposure a few rods
due south. In the main quarry were found Spirifer mucronatus, var. poster us,
otherwise no fossils but Spirophyton.

In the south exposure more fossils were found and these about fifteen
feet below the horizon of the main quarry; as follows:

Pleurotomaria, probably an undescribed species, which may be compared

in general aspect to P/. tri/ix of the Hamilton shales, but is of much larger

* These sections, made in 1895, pertain essentially to the relations of the Ithaca to the Portage fauna. The rocks ot the

Oneonta group have not been observed in this region.
+ In making the observations recorded upon Stations I.-IV., I was accompanied and aided by Professor C S. Prosser, of Union

College. The elevations given for these Stations are barometer measurements by Professor Prosser.

63

64 Report oF THE STATE GEOLOGIST.

size. It bears two strong concentric ridges on the upper surface of the whorl,
and four or five such ridges on the lower surface. Concentric lines fine and
closely crowded. Abundant in a single thin layer.

Pleurotomaria Itys, (vare).

Nucula corbuliformis.

Spirifer mucronatus var. posters.

Liorhynchus mesacostalis.

On the hill next eastward of this quarry and at an elevation of 100 feet
above it, fossiliferous beds appear sparingly to the top. The rocks carry
Atrypa reticularis abundantly, one loose block from the vicinity containing
Leptaena rhomboidalis.

Station If, On the road from Burdick settlement to South Otselie,
Chenango county, one-half mile south-east of the former village, is a long
exposure along the highway and in the banks of a creek which the road
follows. i

The lowest outcrop is of Portage (Sherburne) fucoidal slabs with inter-
vening shale beds, often two or three feet im thickness, but without fossils.

At 207 feet above the creek at DeRuyter, the following fossils were
found :

Spirifer mucronatus, Var. posters ().

Liorhynch us mesacostalis (Cc).

Chonetes scitula (¢).

Tentaculites cf. sproulus.

Palawoneilo constricta.

Paracyclas lirata.

Liopteria levis.

Leptodesma Pogers?.

Nucula corbulitormis.

Station I1f, South Otselic, Chenango county. A road entering the
village from the east runs for a mile or more through a deep gorge which
affords a fine natural exposure, supplemented by several quarries. The
elevation of the South Otselic hotel is eighty-eight feet below the creek at
DeRuyter, and the village is eight miles due south of the latitude of that
place.

At the opening of the gorge on the west, the elevation is forty-five feet
above the hotel. Here the Portage fucoidal layers and sandy slabs (Sher-
burne sandstone) are absent. The first twenty feet are of sandy compact

shales, from which the following fossils were taken :

PLATE Il

UOLEN

HAVANA (

EG al a ae!

|
=)
<x
uw
ve
re
=)
O
ve)
al
O
=
uw

NKQOP HALLENBECK CRAWFORDGO

CLARKE—OnerontTa, ItTHAaca AND PorracE Groups. 65

fTyolithes aclis (ec).

Chonetes lepida (¢).

Strophalosia truncata.

Liorhynchus mesacostalis.

Chonetes scitula.

Productella spinulicosta.

Pholidops Hamiltonie.

Lingula ligea, var. (Hall).

Lunulicardium or Panenka, fragment of a large species.

Abdominal segment of /chinocaris,

Orthoceras sp.

At the top of these beds Hyolithes again appears in considerable abun-
dance, associated with numerous specimens of Léngula ligea, var. (Hall) and

Spirifer mucronatus var, poster us.

Liorhynchus mesacostalis.

Chonetes scitula.

Ch. deflecta.

Nuculites, very short form, cf. Vyssa.

Twenty-five feet above are ten feet of darkish shales, with

Productella spinulicosta.

Strophalosia truncata.

Liopteria levis.

Nuculites cf. Nyssa.

IT!I*. ‘This substation is ten feet above the last horizon, the rocks
heavy bedded argillaceous sandstones which have been quarried for the
purpose of building a catch-basin on the creek near by.

The fauna is highly characteristic and is almost wholly constituted of

typical species of the Hamilton group with the remarkable addition of

g
Leptena rhomboidalis, a species which has not been known to occur in New
York aboye the Corniferous limestone, though it reappears after the close of
the Devonian in the Waverly sandstones of Ohio.

The species obtained are the following :

Lepicena rhomboidalis.

Phacops rana (¢).

Spirifer mucronatus, indistinguishable from the short-winged Hamilton
species (c).

Chonetes scitula, large form approaching C'). deflecta (cc).

Cyrtina sp. nov., large, with smooth exterior and great median septum (c).

9)

66 Report OF THE STATE GEOLOGIST.

Phipidomella Vanuxemi.

Atrypa reticularis, large and finely plicated.

Spirifer asper, widely extended form, much more. alate than that of the
Hamilton group (cc).

Actinopteria Boydi, the typical form of the Hamilton group with fascie-
ulate radii and spinose concentric striz (¢).

Mytilarca with attached Crania.

Grammysia constricta.

Paleoneilo emarginata.

Conularia undulata.

Tentaculites spiculus, small form.

Murchisonia micula.

Poteriocrinus gregarvus.

In the hundred feet immediately overlying this fauna the association
of species is not maintained but only the forms more generally distributed
in the rocks beneath were found, viz. :

Spirifer mucronatus, var. poster us.

Chonetes scitula, Liorhynchus mesacostalis, Nuculites ef. Nyssa and
Palwoneilo fecunda. Phacops rana also occurs in the lower part of this
section, but sparingly, and at the top Paracyclas lirata.

A short distance higher Paracyclas occurs abundantly in soft sandy
shales, the following species being taken at the horizon :

Paracyclus lirata (ce).

Leptodesma Logersi (cc).

Paleoneilo fecunda.

Modiomorpha subalata.

Tropidoleptus carinatus (©).

Chonetes scitula, large form (¢).

Ch. lepida.

Productella spinulicosta.

Tornocerus uniangulare.

In the immediately overlying seventy feet, fossils occur in thin layers at
considerable intervals. Various of these layers were examined, but the asso-
ciations of species were found not to present great variations.

The rocks contain :

Spirifer mucronatus, the normal short-winged form (cc).

Spirifer ; the most abundant species of this genus is a small shell with a
sharp median septum, but with the external aspect of S. mucronatus, var.
posterus. tis probably a variety of S. mesacostalis.

WiVKOOP HALLENBECK CRAWFORD CO.

HAVANA GLEN.

CLARKE—OneEonta, IrHacaA AND Portace GROUPS. 67

Chonetes scitula (c).

Atrypa reticularis, both large and small forms (ce).

Liorhynchus mesacostalis (©).

Cyrtina Hamiltonensis.

Tropidoleptus carinatus.

Actinopteria perstrialis (cc).

A. Boydi.

Liopteria Say?.

Paleoneilo fecunda.

P. emarginata.

Autodetus.

Diaphorostoma sp.

Carapace of Tropidocaris ?

ITI, The first appearance of Spirifer mesastrialis ; elevation 585 feet
above the South Otselic hotel; near the top of the hill, on a tributary to the
main creek.* «

Spirifer mesastrialis, large and. typical (cc).

% z: small variety resembling S. Zu//ius.

Eehynchonella ? eximia ?

Liopteria Greeni.

Tentaculites sp. noy.; a long, slender species, very finely marked with
delicate, subequal rings; not observed elsewhere (cc).

Station ITV. Mineral Spring creek, in the town of Pitcher, Chenango
county, running from Pitcher Springs westward and emptying into the Otselic
valley. The opening of this ravine on the Pitcher highway is about forty
feet below the hotel at South Otselic and four miles south of that place.
The section here, from the mouth of the ravine to its commencement, is 140
feet in height, the rocks, thin sandstones with interbedded sandy shales, ‘The
lower ten feet is a Spirophyton sandstone without other fossils. The beds
above contain associations of fossils at intervals, not varying greatly in their
composition. The fauna as collected from the entire series of the fossil-
iferous bands is as follows:

Tropidoleptus carinatus, common in the lower layers.

Productella spinulicosta (¢).

Cyrtina Hamiltonensis (c).

Chonetes lepida (¢).

Ch. scitula, very large variety (cc).

* This locality was not seen by myself and the list of fossils is drawn from specimens collected by Professor Prosser.

68 Report oF THE STATE GEOLOGIST.

Spirifer, small species with sharp median septum, cf. mesacostalis, var. (cc).

Atrypa reticularis (¢).

Leptostrophia mucronata, the small variety occurring in Cortland county,
more abundantly at Ithaca and in the Seneca lake section.

Paracyclas lirata, common in the lower layers.

Grammysia arcuata.

Paleoneilo emarginata.

P. fecunda (c).

Goniophora Hamiltonensis.

Modiomorpha concentrica (¢).

Actinopteria perstrialis (c).

Pleurotomaria Itys.

Platyceras, small sp. resembling ?. symmetricum.

Cladochonus.

Poteriocrinus gregarvus (¢).

Stictopora Gilberti (cc). ®

Station V. One-half mile northwest of South Otselic, a ravine known as
Madison’s gulf, on the west side of the Otselic river. Elevation of the
lowest exposure, thirty feet above the hotel. Dip section showing a high

angle, estimated at seventy-five feet per mile. Probable difference in eleva-
tion, fifty or sixty feet below lowest strata at Station ITI.

The exposure here which was followed for a thickness of forty feet, con-
sists of unfossiliferous flags and sandy slabs, characterized by ripple marks,
worm and crustacean tracks, fucoidal casts, ete., distinguishing the lower
Portage (Sherburne) beds.

Station VI. DeRuyter; on the south road entering the west end of the
village from the town of Lincklaen, and one-quarter of a mile south of the
cemetery, in a creek running along the road-side, the Tully limestone is
exposed.* Below it the Hamilton shales are shown at the cemetery and in a
fifteen foot bluff a little further south. The Tully limestone is very impure
and schistose below for a thickness of three feet, becoming more compact
above. ‘Top not clear and the Genesee shales not exposed. Directly up the
hill from the Tully exposure, at an elevation of 225 feet, a quarry has been
opened on the land of David Wilcox. This section is in the upper part of
the lower and barren Sherburne sands, and the rocks bear the characteristic
fucoidal and wave marks. A thin, yellowish, compact quartz sandstone bears

Paracyclas liratu sparingly. The immediately overlying layers are softer

* It is also seen two miles east of DeRuyter on the Georgetown road, and one-half mile south of the Otselic stage road.

CLARKE—ONKEONTA, Irnaca AND PortaGe Groups. 69

and more shaly, and contain Spirifer mucronatus var. posterus and Orthoceras
sp. Here also were found three specimens of an interesting species of
_Rhinocaris.*

Station VII. Buel’s creek, one and one-quarter miles east of Truxton,
Cortland county. The exposure here consists at the base, of black, alternating

* Rhinocarzs (?) bipennis, sp.nov. This interesting species has a long and comparatively narrow carapace; in the best pre-
served specimen the two valves appearing to be folded not exactly in the median line. The character of the hinge is obscured by
the manner of folding and it is not possible to determine whether the species possessed a median plate with a hinge on either side
as in true Rhinocaris, or whether the hinge line was actually median as in Hlymocaris, Emmelezoe and Ceratiocaris, but the pre-
sumption from the general aspect of the carapace and from several other structural features, is that the fossil is a Rhinocaris. The
anterior outline presents a somewhat truncate extremity which may have been prolonged into an acute termination as in many
such carapaces, but as the specimen is somewhat broken at this point, its character can not be made out. There is no evidence
ofa movable rostrum. The lateral margins make a broad and low curve of about equal degree before and behind, and posteriorly
the margin seems to have been somewhat truncated or slightly incurved, the specimen being somewhat imperfect here. The
lateral surface of each valve bears a sing!e fine sharp ridge, scarcely developed into such a carina as characterizes the single keeled
genera Echinocaris and Ptychocaris. This ridge makes an ogee curve, tending downward in front and upward behind, becoming
obsolete on the posterior region of the carapace. A very distinct ocular node lies at about one-third of the length of the carapace
from the anterior extremity; at its summit the surface is smooth and bears a well-defined circular optic pit, as in Rhinocaris and
Mesothyra. The ornamentation of the carapace is quite peculiar ; the region above the ogee ridge is marked by elevated, chevron-
shaped or squamose lines which are sharpest at the anterior extremity, becoming more diffuse and less obscure posteriorly. Their
general direction is parallel to the hinge, though they curve around the optic and mandibu’ar nodes. Below this curved ridge the
surface is quite smooth except near the margins where there are a few faint anastomosing lines such as most of the Phyllocarida
possess. The outer margins of the valves are thickened and the surface slightly grooved within them. Besides the optic node
there is a well-defined node just behind it, probably of muscular or mandibular origin and some other ill-defined node-like irreg-
ularities on the surface which are probably due largely to compression. The abdomen is partially obscured at its proximal end,
but shows three segments, the first two comparatively short, the third long, cylindrical and marked with oblique lines. These
segments arc similar in relative size and aspect to those of the Hamilton species, R. columbina, and are a further reason for
assigning this species to the same genus with that. The telson is produced into a spine which appears to have been somewhat
shorter than the cercopods, though it is not complete. One of the cercopods is preserved, a long slender spine, striated as in
Mesothyra and bearing a crenaolated inner margin which was the base of insertion of a setal fimbrie. This is also a feature well
defined in the specimens of the great Mesothyra Oceani, from the Ithaca fauna at Ithaca.

The accompanying sketch shows the described specimen in its natural proportions,

Traces of appendages. One of the specimens has lost the carapace by exposure to weather and shows traces of certain
structures of the inferior surface. Exceedingly little is known ofsuch structures in the fossil Phyllocarida. In an obscure
species from the»Carboniferous concretions of Mazon creek, Illinois, termed by Packard Cryptoze@, Beecher made out traces of
two or three cephalic appendages, which have been described and illustrated by the former writer; and Whitfield has figured
examples of Hntomocaris and Ceratiocaris, showing evidence of thoracic legs. What is here visible in Rhinocaris is not readily
resolvable into agreement with the structure of the living Vedalia, but is described simply as it appears without any «attempt to
homologize the parts.

In this specimen the removal of the carapace has left exposed a portion of the under side coyering rather more than the area
of one valve. The most prominent features of the exposed surface are two angular hemi-lozenge-shaped plates, whose edge is
sharply lined like marginal portions of the carapace (marked Pin the figure). These lie in a somewhat symmetrical position with
reference to each other, but that at the left is more fully retained than the other. The striated, sharply angled margin appears at
first glance to be a lamellate body b7 itself, but closer inspection shows it to be continuous with a smooth area or plate whose out-
line is not very distinctly retained. Behind these lies another smooth somewhat quadrangular area, the margins of which are
thickened, striated and continue] backward. The bodies P P may possibly have teen united into one trapezoidal plate, although
the inner margin of P seems to be partially entire. In front of these plates are five flat and narrow impressions separated by their
ridges. Allare so directed as to converge to the same area. The fifth or last of these impressions seems to have a somewhat
definite outline and to be faintly striated. The general aspect of these markings and their position suggests that they are rem-
n2nts of cephalic appendages, the narrow ridges being the filling of the spaces between them.

70 Report oF THE STATE GEOLOGIST.

with greenish, sandy shales which, with occasional flags, continue to a height
of fifty-five feet. The black shales are so dark that they resemble in many
places the more bituminous beds of the Genesee, though the rock is more
arenaceous than is usual in that formation. The whole series is almost

devoid of fossils, only a single species of Lingu/la, sp. indet., one of a small

Ambocalia and an occasional Rhodea having been seen. These are undoubt-
ra ‘

edly a part of the lower Portage beds.

VI7'. Truxton; hill at the west end of the village. For a distance of
100 feet above the base the shaly beds of Station VII are exposed; at 300 feet
above this is a slightly worked exposure of ten feet of thin sandstones with
softish interbedded shales. No fossils. Loose blocks on the hill sides indicate
the presence, in the section, of Liorhynchus mesacostalis.

VII, Tripoli brook, three-fourths of a mile northwest of the village of
Cuyler, Cortland county, affords an exposure of upper Hamilton shales,
ending abruptly in the Tully limestones, producing falls forty feet in height.
The limestone begins at the bottom with a thin six-inch band, followed by
interbedded shales and thin limestones. The lower portion from the first
limestone layer to the beginning of the compact limestone bed is eleven feet,
the upper and more solid bed measuring six feet. It is interesting to observe
that at the base of the falls, twenty feet below the impure beds, is a limestone
layer, of the same lithological character as that at the top of the falls. This
is highly fossiliferous as are also the upper and six-foot layer, and both
appear to embrace the same fauna. The shale beds separating the lower
limestone stratum from those above contain species of the Hamilton fauna.

Above the Tully limestone are Genesee black shales without fossils. The
exposure is largely covered, but does not exceed, in total, ten feet. Over
them he dark olive sandy shales and fucoidal flags of the lower Portage group.

On the east of Cuyler village, is a prook along the highway entering
from the east, where Hamilton shales are exposed at the foot of the
south hill, the Tully and Portage terraces being well defined on the hill side,
though no exposures are seen. From the brook level to the Tully terrace
is about seventy-five feet.

At Miiller’s brook, two and one-half miles east of Truxton, the Tully
limestone outcrops not far from the Cuyler road. The same rock appears one
and one-half miles south of Truxton on the Goddard farm, west side of the
Tioughnioga river; and also at the opening of the Cheningo creek into the
latter valley, it is seen on the north side of the Cheningo valley in a small run

on the farm of Otis Wicks. the exposure not exceeding one foot six inches.

a

PLATE IV

JACOB'S LADDER, HAVANA GLEN.

> 208

al

CrLarKE—Oneronta, IrHaca AnD PorracEe Groups. ra

The high hill on the south side of the Cheningo valley and which is crossed
in going to Solon, has an elevation of not less than 600 feet above the valley,
and the exposures near the top afford Spirifer mesastrialis.

Station VITTI. Solon, Cortland county. This village lies near the head
of a stream known as Trout brook which empties into the Tioughnioga eight
miles away. The only exposure found in the region is along this brook. The
rock section is about forty feet in thickness and consists at the base of com-
pact, soft sandy shales with abundant fossils, overlaid by more sandy beds
and flags, also fossiliferous. The uppermost layers are made up of heavy
sandstones containing concretionary masses of immense size, such as I
recorded in a previous report as occurring at Greene, above the green and red
Oneonta beds, and have noted elsewhere at Marathon and near Lisle in the
Tioughnioga valley.

These upper beds are not fossiliferous, but the lower strata furnished
the following species :

Cladochonus (ce).

Spiriter mesastrialis, large and normal (cc).

Chonetes scitula, large form (c).

Orthis impressa, large and normal (c).

Microdon bellistriatus, small variety (cc).

Liopteria Greenii (¢).

Atrypa reticularis.

Leptostrophia mucronata.

Tropidoleptus carinatus.

Paracyclas lirata (¢).

Modiomorpha subalata.

Nucula corbuliformis.

Actinopteria perstrialis.

A loose block in this stream furnished Lepteena rhomboidalis, Spiriter
mesastrialis and Actinopteria perstrialis.

Station IX. McGrawville. This village lies in the Trout brook valley,
four miles east of Cortland. The valley here is broad and though there are
streams entering it abundantly from the north, there is but one from the
south. Rock exposures are few on account of the overwhelming amount of
alluvial deposits. The lowest outcrop observed is in the village and along
its southeastern edge on a creek entering the valley from the town of Free-

town, where there is an exposure of thirty feet of compact sandy shale with

72 Report oF THE STATE GEOLOGIST.

Spirifer mesastrialis and Spirifer mucronatus var, posterus. No other outcrop
occurs on this creek in this township.

IX". Brook one mile east of MeGrawville on the farm of Joel Pritchard,
crossing the Solon road, Elevation, seventy-five feet above Station IX. The
section here covers a thickness of about 100 feet, the rocks at the base being
softish, compact, arenaceous shales, with the following species of fossils :

Spiriter mesastrialis (cc).

Ambocelia umbonata.

Liorhynchus mesacostalis.

Spirifer mucronatus var. poster us.

Cyrtina Hamiltonensis.

Cyrtina, large form with plicated sinus; ef. ewrvi/ineata.

Atrypa reticularis (¢).

Leptostrophia mucronata.

Productella spinulicosta.

Eehynchonella ct. eximia.

Manticoceras Patersoni.

Paracyclas lirata.

Bellerophon sp. nov. with large aperture, narrow whorls and fine concen-
tric surface ornament.

Cladochonus (¢).

Melocrinus tricyclus, Katon (sp.); “tricircled encrinite,” of Vanuxem (cc).

Immediately overlying are compact sandstones with

Spirifer Teevis.

Melocrinus tricyclus.

With the exception of the occurrence on Cowles hill, Greene (see
page 37), this is the easternmost appearance of the species, Spirifer levis.
It has, however, been recorded from Hait’s quarry, near East Homer, which
is almost on the same meridian and about five miles to the north.

From this point upward the rocks are much less fossiliferous, evidences
of the “tricircled encrinite” occurring frequently, and the section is termi-

nated by a thin sandstone bearing masses of Stictopora Gilberti. Loose blocks

g
in the stream indicate the not remote presence of Zropidoleptus carinatus
associated with Spirifer mesastrialis.

Station X. Preble, Cortland county. This village lies in the valley plain,
just north of the Junction of the west branch of the Tioughnioga river with a
stream coming in from the west through the town of Scott. An exposure was

observed along a creek. just off the first road running northwest beyond

PLATE V

THE BRIDAL VEIL, HAVANA GLEN.

CLaRKE—Oneonta, IrHAca AND Portage Grovutrs. (es;

Preble village, on the west side of the valley. These beds lie about fifty feet
above the valley road.

At the base are greenish gray compact shales, somewhat arenaceous, con-
taining Buchiola speciosa, Tornoceras uniangulare, Chonetes scitula, Ch. lepida,
-and Cladochonus. Overlying are barren greenish sands. Seventy-five feet
above, on the roadside, are greenish shales without fossils, fifteen feet. On
the east side of this valley, at the hamlet called Baltimore, is an exposure
‘along the road to Truxton. This is thirty feet high and consists of fissile
black and greenish shales devoid of fossils. Above these, at an interval of
forty feet, are greenish shaly sandstones, also without fossils. This outcrop
lies below that first described, and at about the same level as the upper beds
mentioned.

Three-quarters of a mile due north of the village, at an elevation of 200
feet on a hill at the west of this road, is a quarry from which the flagstones
on the village sidewalks were taken. Many of these stones are covered with
fucoidal markings and others are completely filled with OC/adochonus.

Station XI, Marathon, Cortland county. A rock exposure begins two
miles north of Marathon station on the D., L. and W. railroad, or one-fifth
mile north of the mile-post marked “Owego 83 m.” This section is con-
tinued almost to Messengerville, where it is completed in the Virgil creek at
that place.

The base of the outcrop is. of soft, compact shales, very sparsely fossil-
iferous, overlaid by schistose green sandstone with abundant fossils in thin
layers. Above these layers are heavy bedded sandstones of highly concre-
tionary structure, like those observed at Solon. These weather out by
exfoliation into striking shapes and in their lower portion contain countless
numbers of Spirifer mesastrialis, At about the same horizon this fossil again
occurs in a thick calcareous sandstone which it fills to exclusion, and the
association is repeated on a lesser scale in the rocks above. These mesastiia//s
layers are excellently shown along the Virgil creek. The fossils collected in
these layers are:

Spirifer mesastrialis, large and typical (ce).

Leptostrophia mucronata.

Actinopteria Boydi (ce).

Microdon gregarius (¢).

Liopteria Greeni (¢).

Palwoneilo fecunda.

P. maxima (ce).

74 Report oF THE STATE GEOLOGIST.

Nucula, with the form of .V. /irata, but with a finely lineate surface;
much more oblique than .V. corbuliformis (ce).

Modiomorpha concentrica, normal form.

M. concentrica vay. noy., an extremely oblique shell, distinct and new.

M. concentrica, a form intermediate in outline between the two foregoing.

Leda brevirostris. ;
Grammysta magna.

Tentaculites cf, spiculus (ce).

7! sp. long, slender and sharply annulated ; undescribed (c).

Above these heavy-bedded mesastrialis-layers are sandy shales and slabs
from which the following species were collected :

Actinopteria perstrialis (¢).

A. Boydi, very small form (c).

Palwonetlo constricta (¢).

Microdon gregarius (©).

Spirifer mucronatus var, posterus.

Leptostrophia perplana (ce).

Schizophoria impressa (¢).

Station XII, One mile north of Lisle, Broome county, at the narrows of
the Tioughnioga river, seven miles due south of Marathon. Rocks are here
exposed in high bluffs on both sides of the river, but are more accessible on
the east side along the highway than on the west along the D., L. & W. rail-
road, On the east an escarpment of 100 to 125 feet has soft, compact, greenish
argillaceous sandstones at the base. Overlying is a bank of heavy concretion-
ary sandstones, similar to those observed at Station XI, but not less than 300
feet higher, showing the repetition of such formations in these upper beds.
Fossils are very scarce in these beds, in contrast to their abundance at Station
XI. The “tricireled encrinite” (Melocrinus tricyclus), is found throughout
in thin layers, and the following additional species were collected :

Leptostroph ta mucronata.

Spirifer Mucronatus, Var. posterus.

Sp. mesastrialis, small form only.

Atrypa reticularis.

Cyrtina Hamiltonensis.

Schizodus appressus,

Cadochonus

CLARKE—OneEontA, ITHaca AND PortaGe Groups. 75

Seneca Lake Section.

Station XIII. The village of Havana (now called Montour Falls),
Schuyler county. Montour creek enters the village from the west with a ver-
tical fall of 165 feet (Montour Falls, Plate 1); above this are a series of smaller
cascades which together make the total fall of the creek from above the bridge
on the west hill to the village street, 195 feet. The falls proper, or the lower
escarpment, are shown in plate I. The steepness of the rock wall here renders
a close analysis of its composition difficult, but a great part of the series is
exposed in a more accessible condition along the road, which winds up the
hill and crosses the stream above the falls.) As a whole the rocks are greenish,
sandy shales with thin, sandy flags, abundantly marked with crustacean tracks.

The first fossiliferous horizon was found at an elevation of 110 feet above
the main ‘street, and the fossils here occurring re-appear at an horizon just
above the top of the falls (165 feet), in both instances in a soft, argillaceous
shale. The species obtained were:

Ambocelia umbonata (ce).

Spirifer mucronatus, small varicose variety (cc).

Strophalosia truncata.

Productella spinulicosta (cc).

Leptostrophia mucronata (cc).

Manticoceras Paterson (c).

Loxonema ct. Noe.

Cladochonus.

Arthracantha.

Cyclopteris.

Seventy-five feet higher the rocks become much more sandy, heavy layers
of sandstone being frequent, and in two places these have been worked for
flag and foundation stone of an inferior quality. Here Lunulicardium fragile
occurs in great abundance.

Station XIV. Wavana Glen. This well-known and beautiful ravine is
situated one and one-half miles south of the village of Havana, and about
three miles south of the celebrated Watkins Glen, at Watkins, which it equals
in natural beauty. Although the public are admitted to its attractions only
upon the payment of a fee, I was indebted to the proprietors for liberty to
come and go at will, and to make as much debris as was necessary for the
examination I had in hand.

The frequent abrupt cliffs and high falls throughout the gorge do not
facilitate the careful examination of the strata, but the artificial means of

76 Report oF THE Strate GEOLOGIST.

scaling these have often brought otherwise inaccessible points within reach.
The length of the exposure, cutting completely through from near the base of
the Havana valley to the top of the eastern hill makes the detailed section an
important one. As a whole the rocks are highly unfossiliferous. Fossils are
found only at wide intervals in thin layers and in small numbers. This
feature, however, is a characteristic of the strata in this meridian, where the
fauna is distinctly less prolific than in the Cortland and Chenango county
sections of the Ithaca beds and in the typical Portage beds of the western
sections (meridians of Canandaigua lake and the Genesee valley).

The commencement of the rock exposure in the Havana glen lies at the
summit of the delta plain of the stream which rises to no great elevation above
the road.

N/V". The beginning of the rock section affords soft, sandy shales,
containing Buchiola speciosa, shown in the exposure below the entrance house
and in the first falls, known as the “ Portal Cascade” (Plate VI, Dy

Thirty-three feet above the entrance is a band of black, fissile, pyritous
shale, seen on the approach to the first foot bridge, and not far above, in the
escarpment of “ Eagle Cliff” (Plate II), are thin sandy layers with beautiful
specimens of Plumalina plumularia.

XIV?. Atthe top of the “Council Chamber” (Plate VI, 2, 3) and near the
foot of the “Curtain Cascade” (elevation ninety-five feet above entrance) | Plate

IT]

are some compact soft shales in which the following species are found :
Cladochonus (ce).
Ambocelia umbonata.
Cyrtina Hamittonensis.
Atrypa reticularis.
Leptostrophia mucronata.
Paleoneilo constricta.
P. cf. lamellata.
Loxonema Noe.
Diaphorostoma, a small, ventricose, undescribed species occurring in the
Portage fauna of the Naples section.
Manticoceras Patersoni.
NXIV*. Along the bridge approaching the “Curtain Cascade” and at a
slightly greater elevation than the last, occur
Schizophoria impressa.
Centronella Julia. (2)

Atrypa reticularis, small and coarse-ribbed, and large, elongate forms.

"N37 yNWAVH '(SA|X NOILWIS) ANNA] SH] 6

'N31D YNWAVH '(%AIY NOILVLS) S79V4 SNINSdSIHMA “b

‘NS1D WNVAVH ‘(7AIX NOILVLS) YSENVHD TIONNOD §(€

'N31D WNVAVH ‘(4A1X NOIWLS) YSEWYHD TIONNOD -Z
‘"N31D YNVAVH ‘(AIX NOILVLS) S0VOSVD ILyOd ||

IA 311d \

Yen Pkt

“eer . .

CLARKE—OwneEontTA, ITHACA AND PortracE Groups. 77

Productella speciosa.

XIV‘. Soft shales at the base of the last stairs but one leading to the
“Bridal Veil” falls (see Plate V) :

Manticoceras Patersoni.

Loxonema Noe (cc).

Lunulicardium (2), a peculiar undescribed species of a new generic form,
with sharp fasciculate plications and a series of irregular spinous processes on
the anterior margin. This form is not of infrequent occurrence in the Naples
section, both in the Styliola limestone and in the Portage shales. Elevation,
200 feet above entrance.

AIV*®. Soft shalesat the base of “ Whispering Falls,” elevation 242
feet (Plate VI, 4), contain:

Manticoceras Patersoni.

Orthoceras.

Atrypa reticularis.

Cyrtina Hamiltonensis.

Cladochonus.

XIV*. At an elevation of 264 feet above the entrance, is the “Tunnel,” an
opening and passageway along a joint in a projecting cliff (Plate VI,5). Here
occurs a sandy layer with small calcareous concretionary masses, containing

Styliolina fissurella (cc).

Strophalosia truncata.

Chonetes lepida.

Ambocelia umbonata.

Cladochonus.

Twelve feet below this horizon, at the foot of the stairs leading from the
“Tunnel,” occur:

Manticoceras Patersoni.

Chonetes scitula.

Productella spinulicosta (ce).

Cladochonus.

ALIV". “Glen Chaos;” elevation 253 feet. Here has been an interesting
displacement of the rocks, a great mass having fallen along a joint plane for
fully seventy-five feet, filling the gorge with tipturned strata. These dis
placed rocks are, in part, soft, compact shales with fossils, and others are sandy
layers with caleareous concretions containing essentially the same species.
The fossils obtained are

Strophalosia truncata (ce).

78 Report oF THE STATE GEOLOGIST.

Productella spinulicosta (ce).

Leptostrophia mucronata (¢).

Spiriter subumbona.

Chonetes lepida.

Cladochonus.

XTV*. In the bed of the stream, at an elevation of 278 feet, are sandy
layers with some calcareous matter in which C/adochonus is abundant, together
with the following species :

Leptostrophia mucronata.

Chonetes lepida.

Schizophoria impressa, small form.

Buchiola speciosa.

Lunulicardium ? sp. des., with spines (see XTV*),

LL. ornatum.

Above this horizon few traces of fossils were found. At the top of the
“Summit Cascade,” elevation 319 feet (Plate VII), Manticoceras Patersoni
appeared, but no other species were observed. This is the top of the gorge,
the rise beyond this point being very gradual and without striking features or
rock exposures. The top of the hill on the north bank of the stream has an
elevation of 425 feet above the entrance to the ravine.

On the highway going north from Havana to Watkins exposures of the
lower beds shown in the Montour falls escarpment are seen for a mile and a
half. The actual elevation of Havana is about 467 feet A. T.; that is not
more than twenty feet above Seneca lake, from which the water sets back into
the now abandoned Chemung canal as far as the first lock just north of
Havana.

At the salt works on the lake (Salt Point), one and a half miles north of
Watkins, and twenty feet above the lake, where an excavation has been made
for the erection of water tanks, there is an outcrop of sandstone bearing
Cladochorus abundantly. With an allowance for dip of twenty feet per mile,
which is sufficiently large in this section, this outcrop corresponds in elevation
to the stations at XIII and XIV*,

Station XV. At Glenora, on the west shore of Seneca lake, ten miles due
north of Havana, is the mouth of Big Stream, which has cut a deep and rather
difficultly accessible gorge for upwards of two miles. The opening of this
ravine at Glenora is bordered by a high escarpment (125 feet), making a
large and beautiful amphitheatre. The beds are quite regularly alternating

sands and shales, and contain, sparingly, the following fossils:

PLATE VII

Summit CASCADE HAVANA GLEN.

CraARKE—Ownekonta, IrHAcA AND PorracGEe Groups. 79

Manticoceras Patersoni.

Tornoceras uniangulare.

Bactrites.

Spirifer mucronatus, small, varicose form of var. posterus.

Leptostrophia mucronata.

Ambocelia umbonata.

Chonetes lepida.

Paleoneilo muta.

P. ef. constricta.

Cladochonus.

XV". Another exposure favorable for examination lies on the same
stream, where it is crossed by the highway at an elevation of about 425 feet
above the lake, that is, not less than 300 feet above the outcrop last mentioned.
The rocks are soft and in part sandy shales, with a characteristically Portage
fauna throughout, viz. :

Buchiola speciosa.

Cardiola Doris (cc).

Lunulicardium fragile (¢).

Chonetes scitula.

Lingula ct. spatulata.

Bellerophon, resembling an undescribed species from the Styliola lime
stone.

Probeloceras Luther, small variety.

Manticoceras Patersoni.

Tornoceras uniangulare.

Styliolina fissurella.

With proper allowance for dip the horizon of this fauna cannot be far
from that of Station XIV‘ and the higher Lunulicardium beds of XIII.

XV’. At the village of Dundee, Yates county, on the same stream and
at an elevation of 600 feet above the lake, are sandy, unfossiliferous shales
abounding in large, flat clay-iron-stone concretions, having cone-in-cone fully
developed.

Station XVI. The village of Starkey is about two and a half miles east
of Dundee and the same distance north of Station XV. At the elevation of
the Northern Central railroad station occurs a sandstone with Cladochonus.
In similar layers above, the fauna is repeated. It consists of

Cladochonus (ce).

Spirifer mucronatus, small varicose variety.

80 Report oF THE STATE GEOLOGIST.

Cyrtina Hamiltonensis.

Ambocalia wmbonata.

Orthis, sp.? a moderately large form of Dalmanella.

Lunulicardium cf. ornatum.

Manticoceras Patersoni.

Station XVI, Plum creek, running east and west through the village
of Himrods, Yates county, and entering Seneca lake, makes a ravine through
the lower Portage and upper Genesee beds. At the lake (elevation 447 feet
A. T.) are the bituminous beds of the Genesee above the Styliola layer, whose
position in this formation is just about at the lake level. The height of the
Genesee slate in the sides of the ravine is 150 feet, and the beds near the
top bear its characteristic fossils, ¢. ¢.,

Schizobolus truncatus.

Orbiculoidea Lodensis.

Chonetes scitula.

Liorhynchus quadricostatus,

Nucula corbul Z tormis.

Phthonia lirata.

Pleurotomaria rugulata.

Styliolina fissurella.

The Portage beds come in with a gradual change from black to greenish
shales, followed by flags and thick sandstones. At 170 feet occur

Lunulicardium fragile.

Buchiola speciosa.

Cardiola Doris.

Bactrites cf. gracilis.

Probeloceras Lutheri.

Tornoceras uniangulare.

Beneath sandy layers similar to those described at Station XVI occur
shales with Buchiola speciosa at the Northern Central railroad cut, two miles
southeast of Penn Yan; and agai, in close connexion with such beds, one and
a half miles south of Penn Yan, on the road to Branchport, are sandy shales
bearmg Lunulicardium fragile, sixty feet above Keuka lake (elevation 718
feet A. T.).

Station X VITL. Belknap’s gully, two miles north of Branchport, Yates
county. Elevation of mouth of ravine not more than fifty feet above Keuka
lake, A carefully measured section of the exposures here has been given by
Mr. D. D. Luther in the Thirteenth Annual Report of the State Geologist

Crarkrk—Oneonta, ItHaca AND PortTacrE Groups. 8]

(1895), pp- 123-125. The lowest shale beds lie near the base of the Portage
group, and are followed by a band of black shale (“Lower Black band”),
forty feet in thickness, above them lyimg bluish sandy shales with thin flags
(95 feet). The latter shales bear fossils at intervals:

“Ungulina” suborbicularis.

Buchiola speciosa.

Productella spinuticosta.

Above these are 125 feet of sandy shales and thin sandstones, which are
‘apped by a western continuation of the red and green nodular limestone or
“@Goniatite concretionary layer,” which is better developed in the Naples
valley, and has been frequently described by the writer.

Thirty-five feet below this concretionary layer the following fossils were
found :

Manticoceras Patersoni.

Bactrites cf. gracilis.

Bellerophon natator.

Buchiola speciosa.

Lunulicardium ornatum.

I. sp. noy., with extremely fine radial striae, frequent in the Naples
section.

Lucina? ? sp. noy.; fine lined species representing an undescribed
generic form; abundant in the Naples section.

At this poimt, lymg just about half-way (twelve miles) between the
Seneca lake section on the east and the Naples section on the west, the true
Portage or Naples fauna prevails largely to the exclusion of representatives of
the Ithaca fauna. The sections described have clearly shown the gradual
appearance of certain of the more generally diffused species of the Portage
fauna (¢. g., Vanticoceras Patersoni, Buchiola speciosa) as far to the eastward as
the Tioughnioga valley, in the midst of a highly developed Ithaca fauna; the
diminution of the latter with a notable increase of the former in all Seneca
lake stations, and finally a virtual exclusion of the latter, at Branchport,
though we do not find here the more prolific development of the former

attained in the Naples valley and westward.

Norz.—The diagrams given upon page 62 require a word of explanation. The upper curve in each is not a topographic line,
but is employed to facilitate the expression of the varying thickness in the deposits of the Portage epoch. ‘The differential crust
moyements, which are the important factors in this difference in sedimentation, might also have been suggested by a curvature of
the strata underlying the Portage seciments. There is not sufficient difference in the lithologic character of the deposits through-
out their extent to justify an assumption of material diversity in bathymetric conditions. Therefore we regard the Naples region,
one of much less rapid crustal depression than the regions east and west. By introducing the upper curve of these diagrams, at
the base of the Portage sediments, we might have indicated with approximate accuracy such differential depression of the crust
during this later epoch of the Devonian. Such curvatures of the underlying rocks are, however, not yet deducible from recorded
facts. ‘

6

CeOROGICAW SURVEY OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

THE CLASSIFICATION AND DISTRIBUTION OF THE HAMILTON
AND CHEMUNG SERIES OF CENTRAL AND
EASTERN NEW YORK.

BAIT IE.

JAMES HALL, | CHARLES 8. PROSSER,

State Geologist. Assistant.

1895,

ae

sed
=
=
~~
3
=
t

Dr. James Hall, State Geologist.

Sir :—I herewith present my report on the classification and distribution
of the Hamilton and Chemung series of central and eastern New York. T his
report 1s based largely on field work conducted during the summer of 1895.

Respectfully yours,
CHARLES 8S. PROSSER.

Union Cotteck, ScHenrcrapy, Jan. 1, 1896.

85

= ee) ae \ ig ~,! on ae ; / Ea - on ;
“- y “ ; F : i ie RP ana . , ig ee 4 oe ie. 4 a J - a $i
; o) va ; etter asthe ioe) cs y eek <n ne
a i, a -* 1 2 a ly mr « ym G, ra 7 a a » 7 ‘i * +
as ae ; ; ON) Ae ee ae ee © ee ae A ’ hw 9 “
4 ‘ ; oh rs u Dae ee ae rT *, 7 Ps Ge :
: Lig
7 7 7
/

; i} .

/ fi
%

« ;
}
4
# ’
F i
=
j
Fi ~
4
i he
ws.
’ 4
= : s
‘i i;

ORE HITS Te ae
5 =“ \

ok Tes y GEOLOGIC Mee i
soni 1 j ° ARTS z

= i%, ¢ y; =

NGe Tt. nme bya ot ay, CHENANGO, RUSTE, OTSEGO, se
‘ feted Oe. \ aie 3s ae a as swe see | : SCHOHARIE ano ALBANY fa
% Apres 7fizews Yerss vay i = iw er Moh \ ARE ea POR 2; ‘ By. i AY a | ees H 4
Nafta JP xine Sh} MS Vanes We ; : (Ps 7g, a ops ; \ i te ae, YY Oe an kr
wees: A 6 Tihok Ses. CHARLES S. Prosser. IN

Nha, (
ON ee ‘S

CAL, oH

ice

ie

<<
~
=a
i 7
Si
aS

2
-

q

(

me

es
e |
se
Sly

Be

= af z ul

Seve: a
3 ry al
5 l=ByY

we fie.

CSS.
Cot hh
i}

< ay ee i aE Be riya Ca See ah, nies

haul he oe Pe at

; H. fe UIE a Se ies eny) ay san - ve Dnse
NN a p Peat any eg eee oes sas a aN sian NAA Ie he Wk omer ¢ <a
on ME ees
SN Gt ri ca kee at
\ PES f voip S\N TS SMELT ON MEI he) dh See Vie = —/\\ et aVaye oe
D ieccsiatene nee Rye ae age be seve ree ah mr OnE
ANE LE AG ie WS SSA ‘) ON x2 ZY na ac: ae ae I ail Ox estas TPEEY yy Ea 5 ’
he TR: WO Ne PAR pn ea NaN coe oa gel ae BS ina wee ae aise 1H 348
EON Te MATA TN Me A7 isi TT Oe ENT OR ERCP iy. Bice eS ns ee at I ht
Sp taetled RNY |e LHL cape i eNO AE ais Saha ae dito
Sam an (mn oh Cos acs CAN oN qe: e SEE Gl SRR tll C7
ean ani Ban awe SONG O a au: 4 Ze CY SO et Uist | sess ik
of | NY 5 a PO IRS Vas a AN I > bo /\ ach et ia LA
AMY irs Heda apenas (AES SRN Ee
POON NRL. Tee \ HEY NS AGS toon ROUGE.
ANS “HAR t Yio jus A sete SS WA () > we ey hh sla 3 IP, fut H}
ESS ; footie ile 0 mace geese eas Harr
my a ae Wit cm Gi SAT Ms we |
u Saqc (gee aly 7 NT A ] c. A] seenauan
tiny! as 7: WES
ib ead ns cm 3 fils gf AV wal
eee ay GL A fas eur ae, __ PERS <i is ee =

The Classification and Distribution of the Hamilton and
Chemung Series of Central and Eastern New York.

PA Re. -1.

By CuHaries S. Prosser.

ConvEents.—IJntroduction ; Ithaca formation, p. 87; Annual New York Reports, p. 87; Final
New York Reports, p. 90; Views of more recent Contributors, p. 92. Vhe Chenango Valley section:
The formations of Central New York, p. 94; Sangerfield and Madison, p. 96; Onondaga limestone and
Marcellus shale, p. 96; Hamilton formation, p. 96; Hamilton and Brookfield, p. 96; Smyrna, p. 100;
Sherburne, p. 123; North Norwich, p. 187; Norwich, p. 140; Oxford, p. 148; Greene, p. 150; Fenton
and Chenango, p, 154. The Unadilla Valley section : Columbus, p. 167; New Berlin, p. 170; Pittsfield,
p. 178. Geology of Southern Otsego county: New Lisbon, p. 180; Laurens, p. 190; Hartwick, p. 194;
Milford, p. 194; Maryland, p. 204.

INTRODUCTION.

Ithaca formation—During the summer of 1895 the Ithaca formation,
with those immediately below and above, was carefully studied, proceeding
eastward from the meridian of the Chenango river valley until its fauna dis:
appears in Schoharie and Albany counties. <A residence of nine years in
Ithaca made the writer well acquainted with the typical exposures and fauna
of this stage, while other investigations familiarized him with the same series
of deposits in southeastern New York and eastern Pennsylvania. ‘The region
examined in 1895 had not been systematically studied in recent years, and it
proves to be one of the most interesting of the New York Upper Devonian.
However, before entering upon a systematic description of the characters and
distribution of the Ithaca stage, it will be well to review briefly the former
papers describing this formation.

Annual New York Reports—The name Jthaca group' was proposed by
Professor James Hall, in 1839, for a mass of rocks which consists of “ alterna-
tions of shale, both slaty and compact, and argillaceous sandstone,” typically
exposed at Ithaca.” At this time the underlying shales and argillaceous sand-
stones, which were later called the Portage group, had not received a name,
although they were recognized as constituting a group, and their stratigraphic

position was correctly indicated.’ Professor Hall separated the Ithaca group

1In this review the nomenclature of the New York reports is followed.
2 Third Annual Report, Fourth Geological District, New York (Assembly Doc. No. 275, 1839), page 318.
3 Tbid., pp. 302-4, 314.

87

88 Report oF THE STatTE GEOLOGIST.

from the lower one because it differed “in the contained fossils, and in some
particulars of its lithologic character.”' The succeeding formation—the
Chemung—was also named and briefly described in this report,? mention being
made of “a great variety of beautiful and characteristic fossils,” several of
which were generically identified.’

Vanuxem, in 1840, reported flags of excellent quality near Sherburne,
Chenango county, and proposed the name Sherburne flagstones for the
group underlying the Ithaca, stating that, “the stones are of various grades
of thickness, alternating with greenish or olive colored shale,’* and further
that “the flagstone mass” extended from Cayuga lake through the Third
Geological District.’

Immediately following the Sherburne flagstones is the Ithaca group,
which Vanuxem described as “consisting of sandstone and shales, forming a

6 Next came the Chemung group, which
g group,

thick mass, highly fossiliferous.”
‘forms the narrows of the Chemung river, whence its name,” and finally the
Montrose sandstone, or sandstone of Oneonta, which, according to Vanuxem,
‘is the last or upper rock of the Third District * * * [and] is found
in Otsego, Chenango and Broome counties.”* Vanuxem also stated that the
Montrose sandstone covered the whole of the upper part of Susquehanna
county, Pennsylvania, its name being selected because it surrounds the town
of Montrose, in that county. Although not explained in the report of 1840,
the final report by Vanuxem shows that the other term, “sandstone of One-
onta,” referred to the ledges of greenish grey sandstone on the hills near
Oneonta, in the southern part of Otsego county, New York.

Professor Hall spent the field season of 1839 in western New York,
studying the formations of Steuben, Allegany, Cattaraugus, Livingston and
Genesee counties, and in his report we find a classification of the rocks of the
Fourth District, “
a few of the most common and characteristic fossils;” the classification for

giving their order of succession, together with the names of

that part of the series which is now under consideration being as follows :
“Old Red Sandstone.
“Chemung Group.

“ Portage Group.

1Third Annual Report, Fourth Geological District, New York (Assembly Doe No. 275, 1839), p. 318.

2 [bid., pp. 322-324.

3 Tbid., p. 322. :

4¥ourth Annual Report, Third Geological District, New York (Assembly Doc. No. 50, 1840), p. 381.

5 The counties forming the eastern part of the Third Geological District were Fulton, Montgomery, Otsego, Chenango and
Broome, which would imply that the group was regarded as reaching the eastern part of Otsego county.

6 Fourth Annual Report, p. 381.

7 Tbid., p. 381.

ProssER—HAaAmMILTON AND CHEMUNG SERIES. $9

“Gardeau Flagstones.

“Tthaca Group.

“Cashaqua Shale and Sandstone.

“Upper Black Shale [Genesee of the later reports].

“Tully Limestone.

“Moscow Shale;”' the upper division of the Hamilton group of the
later reports.

That which especially claims our attention in the above classification is
the position of this group. Professor Hall clearly indicated the relative
position of the Ithaca group and its extension westward, stating that “in the
order of succession the Ithaca group follows the Cashaqua shale; but in the
Genesee valley, and the counties examined this season, that group | Ithaca |
is entirely wanting, and will probably not be identified farther west than
Seneca lake.”* In the final report the Cashaqua shales, Gardeau sandstones
and Portage group of this report were classed together as forming the Portage
group,’ while the Ithaca group was regarded as forming the lower division of
the Chemung group. Subsequent studies have shown the earlier to be the
more accurate of the two correlations.

In the annual report of 1841, which is the last one of the series, Pro-
fessor Hall said that “the tabular arrangement of strata given at the conclu.
sion of last year’s report, 1s fully borne out by the examinations of the past
season, with the exception of the Ithaca group, which cannot in most parts of
the district | Fourth] be identified as distinct from the Chemung.” ®

Conrad’s report of 1841 contains a table of the New York formations
which he referred to the Silurian system, dividing the system into a lower,
middle and upper series, of which the following formations composed the
upper series :

“26. Oneonta Group.

“95. Cazenovia Group.

“24. Tully Limestone.

“23. Sherburne Group.

“22. Shales near Apulia.
“21. Black Slate.” ®

Several of the formations were evidently named by Conrad, and the

relative succession was not correct in all cases, as for example, with the

1 Fourth Annual Report, Fourth Geological District (Assembly Doc. No. 50, 1840), p. 453.
2 Thid., p. 390.

3 Geology of New York, Part IV, 1843, p. 224.

4 Tbid., pp. 251, 259.

5 Fifth Annual Report, Fourth Geological District (Assembly Doc. No. 15), 1841), p. 179.
6 Fifth Annual Report on the Palaeontology of New York, 1841, ibid., p. 31.

90 REpPoRT OF THE STATE GEOLOGIST.

Cazenovia group, which is a part of the Hamilton formation of the final
classification, and is below the Tully limestone.’ No, 21, the “Black slate” of
Conrad, is the Marcellus shale ; the “shales near Apulia,” “Sherburne group ”
and “ Cazenovia group ” belong to the Hamilton formation, while the “Oneonta
group” belongs to the Ithaca group. The names Sherburne, Cazenovia and
Oneonta groups were apparently proposed by Conrad, and it is important to
observe that Vanuxem, in 1840, used two of these names for formations in a
different sense from that in which Conrad apphed them. The “Sherburne
flagstones,” of Vanuxem, being above the Tully limestone, and in the Portage
group of the final reports; the “Sherburne group” of Conrad, be/ow the Tully
limestone and in the Hamilton group. The “ Oneonta sandstone” of Vanuxem
referred to the heavy greenish-grey and red sandstones in the upper part of
the hills, near Oneonta, while the “Oneonta group” of Conrad, as shown by
the fossils which he described therefrom, was composed of the bluish shales
and sandstones in the /ower part of the hills and along the Susquehanna river
valley, in the vicinity of Oneonta. The Chemung and Catskill groups, Conrad
regarded as belonging to the “Old Red Sandstone” or the Devonian system?

In 1842, Conrad published a paper entitled “Observations on the Silurian
and Devonian Systems of the United States, with Descriptions of New
Organic Remains,” in which he drew the dividing line between the Devonian
and Silurian at the base of the Ithaca group. Conrad stated that “the rocks
of the Ithaca group, Chemung group and the Old Red Sandstone, near Bloss-
burg, in Pennsylvania, constitute the Devonian system as developed in
Europe, and contain a number of the organic remains which characterize the
Devonian, * * * The lower or Ithaca rocks, many hundred feet thick,
contain quite a distinct class of fossils, either from the Silurian below or from
the Chemung strata above. The Chemung rocks, I have ascertained, hold
many forms analogous to the rocks of Devon, which constitute the Devonian
system, and some identical species.” 4

Final New York Reports—The reports of 1841 closed the series of the
annual reports of the New York geologists. Their final reports were the next
publications, those of Emmons and Vanuxem appearing in 1842, and, in the
following year, those of Mather and Hall. The Ithaca group, together with

the formations immediately underlying and overlying it, does not occur in the

1 In reference to the stratigraphic position of the Cazenovia group, see Prosser in American Journal of Science, third series,
Vol XLVI, 1893, p. 214.

2See Prosser in Proceedings American Association Advancement of Science, Vol. XXXVI, 1887, p. 210; and American
Journal of Science, third series, Vol. XLVI, 1893, pp. 214, 215.

4 Fifth Annual Report, Palaeontology New York (Assembly Doc. No. 150, 1841), p 41.

4 Journal Academy Natural Sciences, Philadelphia, Vol VIII, p. 222.

ProsseErR—Hamiton and CuEmuNnG Serres. 9]

Second District, consequently Emmons in his final report does not discuss
their relations.

Vanuxem in his final report referred to the Portage or Nunda group,
the Cashaqua shale, Gardeau and Portage groups and Sherburne flagstone of
the annual reports.

The Ithaca group remained as a distinct formation between the Portage
and Chemung groups. Vanuxem claimed that “the rocks at Ithaca presented
a different mineral appearance from those below, and from those above them ;
being darker colored, and the shaly part coarse, harsh, dull, and less disposed
to be in layers than either of them, containing numerous fossils, which were
wanting in the flags, etc., below; while those of the lower part of the mass at
Ithaca appeared to be different from those of the Chemung group.”*? And he
further said that it was his intention at first “to unite the Sherburne and the
Ithaca masses, not having discovered in the district those leading characters

% *

by which they could be readily distinguished * but finding, on the
contrary, that Mr. Hall was desirous to unite the Ithaca and the Chemung
groups, from the little or no difference which he could perceive between them
in his district, and that the lower masses merited a distinct name, the original
arrangement was retained, and the name of Sherburne changed to Portage or
Nunda group.” ?

In describing the Chemung group, Vanuxem stated that “between the
Ithaca and Chemung group no precise line of division was observed. A high
ridge was seen rising above the inclined plane at Ithaca; the rocks to the
south contained none of the brownish sandstone of the Ithaca, and there were
different fossils noticed in the two; upon these differences the Chemung group
was founded.” *

Mather’s final report, describing the First Geological District or south-
eastern New York, appeared in 1843. Mather states that. the Ithaca and
Chemung groups occur in the First Geological District, and mentions their
oceurrence in the southwestern townships of Albany county, but does not give
any detailed account of the characters or distribution of these formations.

Hall’s final report was also published in 1848, in which the geology of
western New York is exhaustively described. In this report Professor Hall

followed the opinion announced in his annual report of 1841, and referred the

1 Geology of New York, Part III., 1842, p. 172.

2 Thid., p. 171.

3 Ibid., p. 171.

4 Ibid., p. 179.

5 Geology of New York, Part I., p. 317.

6 Tbid., p. 321, townships of ‘‘ Rensselaerville and Westerlo, and a part of Bern.”

92 Report OF THE STATE GEOLOGIST.

Ithaca group to the Chemung, stating that the reason for uniting the two
groups is “the impossibility of identifying them as distinct by any character-
istic fossils.”! To the Portage or Nunda group Professor Hall referred the
Cashaqua shale, Gardeau and Portage groups, and the Sherburne flagstones of
the annual reports.”

On the geologic map of New York, published in 1842, and the agricul.
tural and geologic map, published in 1844, the Portage and Chemung groups
were colored together, the Ithaca group not being mentioned.

Emmons prepared a report on the “ Agriculture of New York,” and
Chapter VI. of Vol. I. is devoted to a classification and description of the
rocks of the State? In describing those formations which are under special
consideration at present, Emmons used the heading, “ Portage, Ithaca and
Chemung groups of the central counties of New York.” 4

It seems that Emmons recognized a considerable difference between the
Ithaca and typical Chemung, as shown by the fossils collected at several
places, but that he was not prepared to actually separate the Ithaca from the
Chemung group. In respect to this classification Emmons said: “ It-would
seem, from a comparison of facts developed by a careful examination, that the
Ithaca group is not equivalent to the Chemung as it is developed at the
Chemung narrows, but rather that it is beneath, and situated between the
Portage and Chemung groups. There is, however, no necessity for separating
the Ithaca from the Chemung group; it is more simple to regard the masses
as parts of one series, in which the inferior and superior may differ in many
points.” ®

Professor Hall, in the descriptions of the fossils from the Ithaca group at
Ithaca and other localities, has adhered to the classification in his final report,
and referred them to the Chemung group.°

Views of More [ecent Contributors—The next important contribution to
the literature of the Ithaca group was the bulletin of Prof. Henry 8S. Williams,
on “The Fossil Faunas of the Upper Devonian,” which bears the date of 1884.
In this paper the characteristics of the rocks near Ithaca and southward into
the typical Chemung of southern New York and northern Pennsylvania are

described, accompanied by lists of fossils from numerous exposures. As a

1 Geology of New York, Part IV., p. 250.

2 Tbid., p. 224.

3 This volume was published in 1846, and Chapter VI., which is called the ‘‘ New York System,’’ comprises 95 of the 371 pages
of the volume.

4 Agriculture of New York, Vol. I., p. 190.

5 Ibid., p. 191.

6 Geological Survey, New York, Palaeontology, Vol. IV., Part I., 1867, Brachiopoda ; idid., Vol. V., Part I., Lamellibranchiata
I., 1884; #bid., I1., 1885.

ProssER—HaAmMILTON AND CHEMUNG SERIES. 93

result of the studies explained in this bulletin and later papers, Professor
Williams regarded the Ithaca group fauna as coming from the eastward and
occurring in the midst of rocks which in western New York are called the
Portage group, these being succeeded by the Chemung group. Professor
Williams summarized the section as follows, beginning with the Genesee slate
at the base of the section on Cayuga lake :

“Ist. Genesee slate fauna.

“2d. Portage group fauna, distributed through approximately 1,300 feet
of strata, but interrupted by the intrusion of the Ithaca fauna and several sub-
faunas.!

“3d, Chemung fauna, occupying at least 1,200 feet of strata.” *

The distribution of the Ithaca fauna is indicated to some extent on a
chart of “Meridional Sections of the Upper Devonian Deposits of New York,
Pennsylvania and Ohio,” by Prof. H. S. Williams, published in 1886. This
paper considers the composition of the Ithaca fauna and its relation to other
faunas, and the author says: “The Ithaca group of the State reports, contains
faunas which I have defined as stages in the successive modifications of the
Hamilton fauna. This set of faunas differs from the Chemung fauna in the
absence of several of its common and abundant species, and by presenting
unmistakable evidences of earlier stages in modification of species which are
near enough alike to be classified under the same specific name.” ®

In 1886, Professor Williams repeated his statement that the Ithaca zone
is separated from the lowest beds containing characteristic Chemung fossils
by about 600 feet of flagey and shaly deposits which contain a few Portage
species. The author's opinion in reference to the relationship of the Ithaca

fauna being expressed as follows: “The Ithaca fauna and its equivalents are

1 This mass of rocks is subdivided as follows by Professor Williams:

inet OniapOason OS LOMER AM OUSDGIOS Et. acttae)s)scclen) |) vicis(eis(ly oyn.e vate =seie;ojelelolels;e ie} ous /e14js\ je ialersls- csiplenie 600!
De MeUN ACA er rertetiaseise ceisenics ites cociemiaie eteiseciciajeleje> ) veislei nie iolaisies 200!

Middle Portace.. <¢@ypical [ithaca 02) .c eles cnc ce ec taweccsecsece PEE DASt aE rete 100/ 450!
ISG INLETS AGS neta ADO CEO TOOrBCESroe | OCDIOTnn CCT RCC Keen rt aire 150!

Owe! EGriaee SANUBTOMEHANG BALES, co ee ccc cece tlere, cence tac cnlnnne anneele bese aivapinsers 250!

1,300’

See Prosser, in Transactions American Institute Mining Engineers, Vol. XVI, 1888, p. 945.

2 Bulletin United States Geological Survey, No. 3, on the ‘‘ Fossil Faunas of the Upper Devonian along the meridian of 76°
30’ from Tompkins county, N. Y., to Bradford county, Pa.,” p. 29. See also statement on p. 20 that ‘‘the study of the order of
the faunas alone in this meridian furnishes strong evidence for the opinion that what I have called the Ithaca fauna, which was
characteristic of the ‘Ithaca group’ of the early State geologists, is geographically a temporary fauna, preceded and followed
by the conditions and fauna generally regarded as belonging to the Portage group.” The following year Professor Williams
said: ‘In the Portage group at Ithaca, as I have already shown, is a rich fauna, not equivalent to the Chemung, but inter-
mediate between it and the Hamilton.” (Proceedings American Association Advancement of Science, Vol. XXXIII, Pt. I],
1885, p. 423.)

3 Proceedings American Association Advancement of Science, Vol. XXXIV, p. 233. This paragraph was condensed and quoted
as follows by Professor Williams in 1891: ‘t'The ‘Ithaca group’ contains a modified Hamilton fauna, which differs from the
Chemung fauna in the absence of some of its most characteristic species.” (Bulletin United States Geological Survey, No. 80,
Correlation Papers, Devonian and Carboniferous, p. 134.)

94 Report oF THE STATE GEOLOGIST.

wanting in the more characteristic of the Chemung species, and its whole
facies links it as intimately with the Hamilton as with the typical Chemung
fauna.” ?

Finally, Williams, in describing the Genesee section of western New York,
says that not a trace of the Ithaca fauna is seen in Wyoming and Allegany
counties. The Cayuga lake section was briefly described in this bulletin, the
author characterizing the Ithaca group as follows: “ A rich fauna, the Ithaca
fauna, is found in that section [Cayuga lake] before the termination of the
Portage fauna, but in its species it resembles both the eastern Hamilton fauna
and the true Chemung fauna. The studies of its species, and of those occur-
ring above, proves that it represents an earlier stage than that of the Chemung
fauna, and that it hes de/ow as well as above deposits containing the genuine
Portage fauna.” *

In 1893, Prosser reviewed the section of the Ithaca group and limiting
formations as exposed near Ithaca, and discussed the correlation of beds of
similar age farther east.? Professor J. M. Clarke, in 1895, reporting on field
work in Chenango county, discussed in a philosophical way the relation of the
Ithaca and Portage groups. The presence of a slightly modified Hamilton
fauna above the horizon of the Tully limestone and Genesee shales in the
Chenango valley region, as noted by Clarke, makes this paper, which later
we will consider more carefully when describing the geology of that valley,

especially important.
THe CHENANGO VALLEY SECTION.

For several reasons it is thought best to first describe the Chenango
valley region before attempting to trace a dividing line between the Middle
and Upper Devonian of central and eastern New York.

The Formations of Central New York.—In central New York, in recent
years, the geologic formations and series composing the Middle and Upper
Devonian have generally been given as follows, the base of the list being the
oldest :

1 American Journal of Science, third series, Vol. XXXII., p. 198.

2 Bulletin United States Geological Survey, No. 41, on the ‘‘ Fossil Faunas of the Upper Devonian, the Genesee Section, New
York,” p. 238. The date of the publication of this bulletin is given as 1887, but owing to the delay in the Government Printing
Office it was not published until near the close of 1888.

> American Journal Science, third series, Vol. XLVI., p. 217.

4Thirteenth Annual Report State Geologist [New York] for the year 1893 (1895), pp. 552-557.

Norr.—Since this paper was written Mr. Edward M. Kindle has published a bulletin on ‘‘ The relation of the fauna vf the
Ithaca group to the faunas of the Portage and Chemung” (Bulletins American Palaeontology, Vol. II., December 25, 1896, 56 pp ,
3pls.) In this bulletin Mr. Kindle givesa review of the Upper Devonian in New York, which is followed by a description of
ten sections in the vicinity of Ithaca, together with lists of species occurring in the Portage and Ithaca groups He concludes
that the fauna of the Ithaca group shows “a closer relationship to the Portage [than to the Chemung], and should be classed in
the Portage epoch.”’ (p. 49)

ProssER—HamiILtron AND CHEMUNG SERIEs. 95
“Catskill formation.
! | Chemung formation.
Mem SCTICS a5 oi east ow we 2 ees ass - 3
Oneonta sandstone.
| Portage formation.
“Genesee slate.
| Tully limestone.
| author cee a : : ;
Hamilton formation.

Marcellus shale.

The base of the Hamilton series throughout Pennsylvania and New
York is usually sharply defined by the base of the black Marcellus shale
which rests on a massive light grey limestone known as the Corniferous or
Onondaga formation. In western New York, and as far east as the Chenango
valley, the top of the Hamilton series is also clearly marked by another black
shale—the Genesee. Some geologists have considered the Genesee shale or
slate a part of the Hamilton series, and so the top of the Genesee has marked
the line of separation between the Hamilton and Chemung series. Other
geologists have considered the Genesee as the base of the Chemung series,’ in
which case the Jase of the Genesee slate became the line of separation
between the Chemung and Hamilton series.

~ From the Chenango valley west into Ontario county? the Hamilton for-
mation is terminated by the Tully limestone, a somewhat argillaceous lime-
stone ranging from a few feet to thirty-five or more feet in thickness.? The
Genesee slate accompanies the Tully limestone as far eastward as the Chenango

valley, but apparently the limestone and shale do not extend to the east of

1 See Dana’s Manual of Geology, 4th ed., 1895, p. 602. Prof. H. S. Williams, as reporter of the American sub-committee on
the Upper Palaeozoic (Devonic) for the International Congress of Geologists, said: ‘‘ There can be no reason whatever for dividing
the Genesee from the Portage, for in the typical section recurrences of the Genesee lithological conditions occur up to the very
base of the Portage sandstones, which terminate the Portage group of the New York system.” (@ongrés -Géologique Interna-
tionale. Compte Rendu, 4° Sese., 1891, Appendix A, p. 143 [p. C 23 of the copies printed in 1888 by the American committee].
Also see p. A 145.) Professor Williams was also inclined to refer the Tully limestone to the Portage, for he said: *tIn order to
adapt our usage to the accepted usage of European standards, when speaking of Upper and Middle Devonian, we should include in
the Upper Devonian the Genesee shale and so much of the Tully as contains the Rhynchonella venustula fauna.” (Ibid., and see
p. A145.) This opinion was also advanced by Professor Williams in his paper on “‘The Cuboides Zone and Its Fauna;ra Dis-
cussion of Methods of Correlation,”’ where he concludes with the following statement : ‘‘ Therefore, if we wish to express precise
correlation in our classification of American rocks, the line between Middle and Upper [Hamilton and Chemung] Devonian forma-
tions should be drawn at the base of the Tully limestone, to correspond with the usage of French, Belgian, German and Russian
geologists.’ (Bulletin Geological Society America, Vol. I, May, 1899, p. 499.)

2 For the western limit of the Tully limestone see Professor Hall’s statement: ‘* This rock is virtually absent at all places west
of Canandaigua lake ’? (Geology of New York, Part IV., 1843, p. 213). Also the Geological Map of Ontario county, New York, by
J. M. Clarke, on which it is represented as not reaching Canandaigua lake. The author says ‘‘the rock disappears entirely in
Gorham some miles before reaching the east shore of Canandaigua lake ” (Report State Geologist [New York] for 1884, 1885, p. 17)-
It has more recently been shown by D. D. Luther, that the westernmost outcrop of this limestone is about one mile from Gage’s
Landing, on the east shore of the lake mentioned, and that its place in the rock series from this point westward to Erle county is
taken by a thin stratum of iron pyrites (Thirteenth Report State Geologist [New York] for the year 1893, Vol. I., pp. 38-42, 1894).

3 Professor H. S. Williams says: ‘‘ From a few feet to over fifty feet’? (Bulletin Geological Society of America, Vol. I., p. 487).
Professor S. G. Williams gave the greatest thickness as on Skaneateles lake, where he measured two sections, one twenty-five feet
four inches, the other twenty-eight feet two inches, and at Tinker’s Falls, ‘‘ twenty-six or thirty-seven and one-half feet, accord-
ing as one includes or excludes the impure mixed top and bottom portions” (Sixth Annual Report State Geologist [New York]

for 1886, 1887, p. 20).

96 Report oF THE STATE GEOLOGIST.

that valley... From the above statements it may readily be seen that the
section of the Chenango valley is a very important one as regards the classifi-
cation of the Middle and Upper Devonian, especially as to where the line
separating the two series is to be drawn. On this account it is considered
advisable to describe somewhat fully all the formations exposed along the
river valley, beginning with the base of the Middle Devonian, the Marcellus

shale, and closing with the Chemung group near Binghamton.

Sangerfield and Madison.

The eastern branch of the

Onondaga Limestone and Marcellus Shale.
Chenango river rises in the eastern central part of Sangerfield township,
Oneida county. The greater part of the township is covered by rocks belong.
ing to the Marcellus and Hamilton formations. The Onondaga limestone
crosses the northern line of Sangerfield township near its central part, but soon
returns into Marshall township for a short distance, and then cuts across the
northwestern corner of Sangerfield, and extends halfway across the northern
part of Madison township before it again turns northerly. In the northern
part of Madison township the Marcellus is mostly covered, and there are but
few exposures.

Hamilton Formation—The lower part of the Hamilton formation, which
consists of thin sandstones alternating with arenaceous and argillaceous shales,
is better exposed than the Marcellus. The hill north of Solsville shows
coarse, arenaceous shales containing large fossils, and also a sandstone stratum,
two feet in thickness, which was quarried and used in the construction of the
Chenango canal. Above the sandstone and arenaceous shales are blocky
argillaceous. shales, in which Liorhynchus is quite common, but other fossils
are rare. “The shales contain many small concretions which, on weathering,
become considerably iron stained. Near the base of the hill, one-half mile
southwest of Madison village, are ledges of coarse, arenaceous shales, in which
Spiriter granulosus (Con.) Hall, Stropheodonta, Chonetes and large Lamelli-
branchs occur.

Hamilton and Brookfield.

Six miles south of Madison is Hamilton, a classic town to the geologist,

c

since Vanuxem first applied the name Hamilton group to the exposures of
rock in the vicinity of this village, stating that “West Hamilton [now Ham-

1It is true that Vanuxem reported the Genesee slate at North New Berlin (correctly New Berlin) (Geology New York, Part
ITI., 1842, p. 292), which is in the Unadilla valley, some thirteen miles southeast of the last place noted in the Chenango valley, but
careful search in the vicinity of New Berlin failed to reveal the Genesee slate, although there is an excellent exposure showing
the contact of the Hamilton and Portage.

Pross—ER—HaAmiInton AND CHEMUNG SERIES. Q?

ilton | is the locality where it is well characterized.” ' On University Hill are
several exposures of arenaceous shales and thin sandstones. About eighty
feet above the main buildings of Colgate University is a small excavation in
fairly coarse, arenaceous shales, in which Rhynchonellas are common. Near
the summit of the hill is the large university quarry, with an exposure of
twenty feet of shales and sandstones. Coarse, arenaceous shales predominate
in the upper part of the quarry with thin sandstone strata, which were used for
the older university buildings. In the middle and lower part of the quarry
the sandstones are thicker and of better quality. The stone in the laboratory
building came from the middle part of this quarry, and that in the theological
hall from the bottom of the quarry, which furnishes a blue sandstone, eight
inches or more in thickness. Fossils are common, particularly in’ certain
layers, the most abundant being Spirifer mucronatus (Con.), Bill., some of the
specimens of which are very much extended along the hinge line, representing
the extremely mucronate form of the species; Ambocelia wmbonata (Con.),
Hall, and Tropidoleptus carinatus (Con.), Hall. This quarry is supposed to
be the one described by Vanuxem when he said: “At the top of the hill,
about twenty feet of sandstone and shale are exposed. * * * Fossils are
numerous at the quarry, among which are the mucronated delthyris | Sp/r/fer
mucronatus (Con.), Bill.|, the one figured in the wood-cut being from this
locality.”* The figure of the Sp/r/fer just mentioned® indicates that it is one
of the strongly mucronate forms similar to those which I have mentioned as
occurring in this quarry.

To the east of Hamilton township is Brookfield township, the geology of
which has been carefully studied by the writer. Near the village of North
Brooktield, in the valley of the East Branch of the Chenango river, and eight
miles north of east of Hamilton village are excellent exposures of the rocks in
the lower and middle part of the formation. Somewhat arenaceous shales in
the bed of a small brook just north of the village contain numerous specimens
of Ambocelia umbonata (Con.), Hall, but other fossils are not abundant. The
species noted from this brook are as follows :

1. Ambocelia umbonata (Con.), Hall.
2. Productella Shumardiana, Hall.
3. Strophalosia truncata, Hall.

1 Fourth Annual Report, (Assembly Doc. No. 50,) 1840, p. 890. Also see the description of the Hamilton group in Vanuxem’s
Final Report, 1842 (Geology New York, Part III., p. 157). Again, under the description of the formations of Madison county,
Vanuxem wrote: ‘‘The hill at the seminary [now Colgate University] is the most favorable point for the examination of the
group [Hamilton] as it appears in the county.’’ (Jdid., p. 276.)

2 Geology of New York, Part ITI., 1842, pp. 157, 158.

3 [bid , Fig. 3, p. 150.

98 Reporr or tHe Srare Gro.oaist.

4. Rhynchonella (Camarotachia) prolifica, Hall.
5. Tropidoleptus carinatus (Con.), Hall.

6. Spirifer mucronatus (Con.), Bull.

7. Paracyclas lirata (Con.), Hall.

8. Nuewla Randalli, Hall.

9. Homalonotus De Kayi (Green), Emmons.

10. Grammysia, sp.

Near the highway from North Brookfield to Brookfield, about one and
one-half miles east of North Brookfield, is a small quarry with five feet of
massive bluish-grey sandstone at the base, capped by coarse arenaceous shales.
The shales are fossiliferous, the fauna being as follows :

Fhynchonella (Camarotechia) sappho, Hall.
Fehynchonella (Camarotachia) congregata (Con.), Hall (2).
Chonetes coronata (Con.), Hall.

Lingula ligea, Hall (2).

Orbiculoidea (Roemerella) grandis (Van.), Hall and Clarke (?).
Spiriter audaculus (Con.), Hall.

Spiriter mucronatus (Con.), Bull.

Modiomorpha complanata, Hall.

Grammysia bisuleata (Con.), Hall (2).

Goniophora Hamiltonensis, Hall.

Cimitaria recurva (Con.), Hall.

12. Tentaculites attenuatus, Hall.

13. Orthoceras constrictum, Van. (2).

a
Fee ate SO Oe SN, Coe htt we hos ire,

14. Crinoid stems.

In the upper part of the high hills near North Brookfield are dark
argillaceous shales in which fossils are abundant. The outlet of Gorton lake,
east of the village, exposes eighty feet of these soft shales, which have furnished
the following species :

1. Stropheodonta perplana (Con.), Hall.
2. Athyris spiriferoides (Katon), Hall.
Spirifer audaculus (Con.), Hall.
4. Spirifer mucronatus (Con.), Ball.
5. Spirifer granulosus (Con.), Hall.

~

6. Rhynchonella (Camarotechia) prolifica, Hall.
7. Orbiceuloidea Doria, Hall.
8. Ambocelia umbonata (Con.), Hall.

9, Nucleospira concinna, Wall.

ProssER—HamILTon AND CHEMUNG SERIES. 99

10. Vitulina pustulosa, Hall.
11. Chonetes coronata (Con.), Hall (?
12. Orthoceras constrictum, Van.
13. Orthoceras subulatum, Hall.
14. Orthoceras nuntium, Hall.
15. Paracyclas lirata (Con.), Hall.
16. Grammysia bisulcata (Con.), Hall (?).
17. Actinopteria decussata, Hall.
18. Pterinea flabellum (Con.), Hall.
19. Phacops rana (Green), Hall.
20. Homalonotus Dekayi (Green), Emm.
21. Hawosites Hamiltonia, Hall.
22. Paleoneilo constricta (Con.), Hall.
23. Nuculites oblongatus, Con.
24. Tellinopsis subemarginata (Con.), Hall.
. Nucula Randalli, Hall.
Nyassa arguta, Hall (?).
. Nuculites triqueter, Con.
. Nucula bellistriata (Con.), Hall.
Eleven miles southwest of North Brookfield, and six miles south of

bo bo bo
aI D> oO

bo
ioe)

Wemition: is Earlville, situated between the East and West Branches of the
Chenango river, and on the Madison-Chenango county line. The two branches
of the river are a mile apart, forming a broad valley with but few exposures
of bed rock in the vicinity of the village. About one-half mile northeast of
the village near the top of the low hill, is the White quarry, in which about
twenty feet of sandstones and arenaceous shales are exposed. The best
building stone, a bluish sandstone, is near the bottom of the quarry, and about
five feet above the bottom is a stratum composed almost entirely of shells,
largely Rhynchonellas, which is called a “ fire stone,” and higher is another
similar stratum. Spirifer granulosus (Con.), Hall, Tropidoleptus carinatus
(Con.), Hall, and Rhynchonella are common in the quarry.

The best exposures near Earlville are to be found, however, in the cut
on the old Syracuse and Chenango Valley railroad (now called the Chenango
Branch of the West Shore railroad), a little over a mile above the Ontario
and Western railroad station at Earlville. The cut is twenty-five feet deep
in places, through dark blue, blocky shales which, on weathering, crumble
to small pieces. The shales are also well exposed in the gorge of the

brook at the same place. These shales underlie the coarse shales and

100 REPoRT OF THE STATE GEOLOGIST.

sandstones of the White quarry, northeast of Earlville. Fossils are abun-
dant, mainly small forms, although Sp/rifer granulosus (Con.), Hall, is
common. The small Lamellibranchs are the abundant and characteristic
fossils of this zone, especially the Wweu/ide and species of similar habitat, and
the locality is well known to some collectors of Hamilton fossils.

The gorge in Kingsley’s brook at Randallsville, four miles above Ear!-
ville, is another excellent locality for collecting. The rocks are blocky,
moderately coarse arenaceous shales, which form cliffs twenty-five to thirty
feet high along the brook. Fossils are common, especially Ambocelia umbo-
nata (Con.), Hall, and Liorhynchus multicosta, Hall, while in the finer shales

Spiriter’ mucronatus (Con.), Bill., is abundant.

Smyrna.

Three and one-half miles southwest of Earlville is the village of Smyrna,
in Smyrna township, whieh is in the northern tier of townships of Chenango
county. The upper part of the Hamilton formation is well exposed in the
brooks near Smyrna, especially along Pleasant brook from the village north-
westerly.

In drawing the line of separation between the Hamilton and Portage
formations in central New York, Smyrna township is an important region
since it embraces the easternmost extension of the Tully limestone. To
the east of this township and the Chenango valley, the calcareous conditions
of deposition disappeared and the horizon of the Tully limestone is repre-
sented by shales or argillaceous sandstones. Vanuxem, in 1842, mentioned
the occurrence of the Tully limestone in “the northwestern part of Smyrna,” ?
and stated that it had “not been seen beyond the town of Smyrna in an east
direction.” * Prosser, in 1887, recorded its presence and thickness near Upper-
ville, on the south side of Pleasant brook, about two miles northwest of
Smyrna village.* At this locality the limestone is capped by twenty feet of
black, argillaceous shales of the Genesee. In the same year, Professor 8. G.
Williams published a paper on the “Tully limestone, its distribution and its
known fossils,” in which this locality is described,’ and the map accompanying
the report showing “The geographical distribution of the Tully limestone in
central New York,” indicates the eastern end of the Tully limestone at this

locality.’

1 Geology of New York, Part ILI, p. 292.

2 [hid., p. 164

3 Proceedings American Association Advancement of Science, Vol. XXXVI, p. 210.
‘Sixth Annual Report State Geologist [New York] for the year 1886, p. 18.

» Thhd., map facing p. 28.

Prosser—Haminton AND CHEMUNG SERIES. 101

Prosser, in 1893, reviewed the evidence in relation to the presence of the
Tully limestone near Smyrna, and showed that the higher fossiliferous zones
at Norwich and Oxford, twelve and nineteen miles farther south must occur
above the top of the Hamilton, instead of forming the upper part of the
Hamilton formation.’ Finally, J. M. Clarke, in 1894, has shown the same
stratigraphic relations for the rocks somewhat farther west in the northwestern
part of Chenango county.

The various streams and steep hills of Smyrna township afford good
exposures of the rocks, and on account of the importance of this locality in
determining the line of separation between the Hamilton and Chemung series,
the sections along Pleasant brook and other streams were carefully examined.

XVIIT D.? East of Smyrna village are exposures along the small
brook which enters Pleasant brook from the north, below the railroad station,
about two miles west of the Chenango river. The lowest exposures on the
brook, D’, are only a few feet above the level of the railroad. They are
generally somewhat coarse, arenaceous, blue shales, certain layers of which
contain abundant fossils. There are, also, occasionally, thm and irregular
strata which are quite calcareous, but not very fossiliferous. The fauna
is as follows:

1. Tropidoleptus carinatus (Con.), Hall. (cy
2. Spirifer mucronatus (Con.), Bill. (c)
3. Spirifer audaculus (Con.), Hall and Clarke =
CSpiriter medialis, Hall). (1)
4. Nucleospira concinna, Hall. ar)
5. Spirifer granulosus (Con.), Hall and Clarke. (ar)
6. Athyris spiriferoides (Katon), Hall. (r)
7. Stropheodonta perplana (Con.), Hall. (11)
8. Stropheodonta demissa (Con.), Hall. (rr)
9. Stropheodonta concava, Hall. (11)
10. Strophalosia truncata Hall (?). (1)
11. Chonetes setigera, Hall (?). (IT)
12. Modiomorpha concentrica (Con.), Hall. ar)
13. Modiomorpha mytiloides (Con.), Hall. (rr)

14. Modiomorpha subalata (Con.), Hall. (1)

1 American Journal of Science, Third Series, Vol. XLVI, pp. 218-222.

* Thirteenth Annual Report State Geologist [New York] for the year 1893, p. 553.

3 The system of numbering used in this paper is as follows: To the general region about some village, which may be used as
acenter of operations, is assigned a number which is called the station number, as XVIII is the station number for Smyrna.
Then the various sections receive a letter, different strata or zones of which are indicated by primes

+The relative abundance of the species is indicated as follows: aa = very abundant; a — abundant ; ce — very common ;
© = common ; rr = very rare; r = rare.

102 Report oF THE Svrate GEOLOGIST.

15. Microdon (Cypricardella) bellistriatus (Con.), Hall. (x)

16. Paracyclas tenuis, Hall. (r)
17. Palwoneilo constricta (Con.), Hall. (rr)
18. Nuculites oblongatus, Con. (ar)
19. Schizodus, sp. (rr)
20. Macrodon Hamiltonie, Hall. (rr)
91. Pholadella radiata (Con.), Hall. (rr)
22. Orthonota carinata, Con, (rr)
23. Pterinea flabella (Con.), Hall. (rr)
24. Cimitaria elongata (Con.), Hall. (17)
25. Bellerophon, sp. (Vr)
26. Platyceras (?), sp. (ir)
27. Trilobite, sp. (fragments). (rr)
28. Orthoceras sp. “vagments). (r)

29. Plant stems.

XVIII J». A little farther up the creek are falls, some twenty feet
high, and a gorge, the sides of which are thirty feet or more in height. These
shales are much coarser than those of D', and contain fossils of large size, as
Spiriter granulosus (Con.), Hall, and large Lamellibranchs are common.
Alternating with the coarse arenaceous shales are somewhat calcareous layers

and these thick strata form the falls. ‘The following species were collected :

1. Chonetes scitula, Hall. (a)
2. Chonetes coronata (Con.), Hall. (ar)
3. Tropidoleptus carinatus (Con.), Hall. (c)
4. Spirifer mucronatus (Con.), Bill. (c)
5. Spirifer granulosus (Con.), Hall and Clarke. (c)
6. Stropheodonta perplana (Con.), Hall. (rr)
7. Orthis Vanuxemi, Hall (?). (rr)
8. Productella, sp. fragments). (rr)
9. Pholadella radiata (Con.), Hall. (ir)
10. Pterinea flabella (Con.), Hall. (1)
11. Modiomorpha concentrica (Con.), Hall. (vr)
12. Pectenide (a large specimen). (ar)
13. Bellerophon, sp. (rr)
14, Bryozoa. (1)

The lithologic appearance of these shales agrees with that of the upper
Hamilton formation while the fauna is distinctively Hamilton, so that these

shales unquestionably belong to the Hamilton formation.

ProssER—HaAmILron AND CuremuNG SErIEs. 103

XVIII F. By the highway at the eastern end of Smyrna village are
exposures of somewhat coarse arenaceous shales which contain many fossils.
The most abundant species are Spirifer granulosus (Con.), Hall and Clarke,
and 7ropidoleptus carinatus (Con.), Hall, of the Brachiopods ; Nucu/ites tri-
queter, Con., of the Lamellibranchs, and associated with these are numerous
species of Fucoids—the Spirophyton. The complete fauna observed is as

follows:

1. Spiriter granulosus (Con.), Hall and Clarke. (c)
2. Spiriter mucronatus (Con.), Bill. (1r)
3. Spiriter audaculus (Con.), Hall and Clarke. (rr)
4. Tropidoleptus carinatus (Con.), Hall. (c)
5. Cyrtina Hamiltonensis, Hall. (r)
6. Chonetes coronata (Con.), Hail. (r)
7. Chonetes deflecta, Hall. (1)
8. Chonetes setigera, Hall (¢). (rr)
9. Chonetes scitula, Hall (¢). (11)
10. Atrypa reticularis (Linné), Dal. (rr)
11. Orbiculoidea, sp. (1r)
12. Stropheodonta perplana (Con.), Hall. (1)
13. Orthis Vanuremi, Hall. (rr)
14. Nuculites triqueter, Con. (c)
15. Nuculites oblongatus, Con. (1)
16. Paleonetlo constricta (Con.), Hall. (ar)
17. Schizodus appressus (Con.), Hall. (Tr)
18. Paracyclas tenuis, Hall. (11)
19. Phthonia sectifrons (Con.), Hall. (ar)
20. Nucula belistriata (Con.), Hall. (rr)
21. Modiomorpha mytiloides (Con.), Hall. (r)
22. Orthonota carinata, Con. (ir)
23. Microdon (Cypricardella) tennistriatus, Hall. (rr)
24. Macrodon Hamiltonia, Hall. (rr)
25. Lellinopsis subemarginata (Con.), Hall. (rr)
26. Orthonota (2) parvula, Hall. (rr)
27. Sphenotus truncatus (Con.), Hall (4). (rr)

Too imperfectly preserved to admit of positive identification.
It might be S. arceformis.
28. Grammysia arcuata (Con.), Hall. (r)
29. Glyptodesma erectum (Con.), Hall. (rr)

104 Rereorr oF THE Strate GEOLOGIST.

Ds Liopteria, Sp. (ar)
31. Pleurotomaria capillaria, Con. (1)
Boe Cyrtolites (Cyrtonella) pileolus, Hall (¢). (c)

Not well enough preserved to be positively identified. It may

be ( mitella, Hall.

33. Bellerophon crenistria, Wall. (rr)
34. Bellerophon leda, Hall. ar)
35. Homalonotus DeNayi (Green), Emmons, fragments. (rr)
36. Dalmanites (Cryphwus) Boothi (Green), Hall. (rr)
37. Orthoceras, sp. (fragments). (1)
38. Crinoid, sp. (portion of a calyx in several pieces). (rr)
39, Plant (a fragment). (rr)

SECO OY SOOM BACK OF PLEOS-
OWT BRI, D4 WULES ABE

STMYRNG.

(*\8 0.)
=e SURRBUAIE.
= Phin Sandstones Oud Shales.

Coveyed

a GENESEE Shale.
Covered.

‘ e.
= {9 So eee Swoleos. \y hick,

N VIII A‘. Pleasant brook flows through the southern part of Smyrna
village and along this part of the stream are rocky banks affording excellent
exposures of the upper Hamilton rocks. The lowest outcrops studied are a
short distance below the New York, Ontario and Western railroad station,
and about at its level, or approximately 1,127 feet A. T. Fossils are quite
common, the following species having been collected at this locality :

Ih. Tropidoleptus carinatus (Con.), Hall. (c)
9. Ambocalia wnbonata (¢ Jon.), Hall. (c)

Pross—Er—HaAminton AND CHEMUNG SERIES. 105
3. Chonetes coronata (Con.), Hall. (r)
4. Chonetes setigera, Hall. (ce)
5. Chonetes mucronata, Hall (4). (‘)
6. Spiriter mucronatus (Con.), Bill. (c)
7. Spiriter audaculus (Con.), Hall and Clarke. (rr)
8. Spiriter fimbriatus (Con.), Bill. (11)
9. Orthis (2). (rr)
10. Diseina. (rr)
11. Nueula bellistriata (Con.), Hall. (1)
12. Nucula corbuliformis, Hall. (ir)
13. Nucla lirata (Con.), Hall. (1)
14. Paleoneilo constricta (Con.), Hall. (rr)
15. Microdon (Cypricardecla) bellistriatus, Con. (1)
16. Pholadella radiata (Con.), Hall. (1r)
17. Orthonota (2) paroula, Hall. (rr)
18. (4) Modiclla pygmea (Con.), Hall. (rr)
19. (2) Phthonia sectifrons (Con.), Hall, fragments. (11)
20. Tellinopsis subemarginata (Con.), Hall. (1)
21. Schizodus appressus (Con.), Hall. ar)

22. Orthoceras, fragment.

23. Bellerophon, fragment.

XVIII A*. Along Pleasant brook, above the highway bridge in Smyrna
village, is a rather narrow gorge with rocky banks thirty feet or more in
height, extending for a quarter of a mile up the brook. The rocks consist of
coarse arenaceous shales, alternating with sandstones. All the layers are more
or less fossiliferous, and the shales contain abundant fossils. The bottom of
the gorge is about twenty-five feet above the level of the railroad station, or

ry

with an approximate altitude of 1,150 feet A. T. On account of the consider-
able number of species contained in these rocks, some time was spent in
collecting, and the specimens found in the lower, middle and upper parts of
the glen were kept separate. The following lists will give a fair idea of the
species contained in thirty or forty feet of upper Hamilton rocks in the
Chenango valley region. From the lower part of the glen the following
species were collected .

1. Ambocelia umbonata (Con.), Hall. (aa)

2. Spiriter fimbriatus (Con.), Bill. (ce)

3. Spiriter granulosus (Con.), Hall and Clarke. (a)

4. Spirifer audaculus (Con.), Hall and Clarke. (c)

106 Report OF THE State GEOLOGIST.

a9 Spiriter INUCLONATUS (Con.), Bill. (c)

6. Tropidoleptus carinatus (Con.), Hall. (aa)

7. Chonetes coronata (Con.), Hall. (cc)

8. Chonetes deflecta, Hall (2). (7)

9. Chonetes sp. (1)
10. Atrypa reticularis (Linné), Dal. (rv)
11. Athyris (Spirigera) spiriferoides (Eaton), Hall. (1r)
12. Orthis Vanuremi, Hall. ar)
13. Stropheodonta perplana (Con.), Hall. ar)
14. Stropheodonta concava, Hall (2). ar)
15. Orthothetes Chemungensis (Con.), Hall and Clarke. (1)
16. Liorhynchus multicostus, Hall. (rr)
17. Rhynchonella sp. (rr)

Possibly 2. prolifica, H. Very imperfectly preserved.

18. Productella sp. (very imperfect specimens). ()
19. Cyrtina Hamiltonensis, Hall (?). (rr)
20. Cimitaria recurva (Con.), Hall. (rr)
21. Paracyclas tenuis, Hall. (rr)
22. Palwoneilo emarginata (Con.), Hall. (r)
23. Palwoneilo constricta (Con.), Hall. (ar)
24. Schizodus appressus (Con.), Hall. (ar)
25. Nuculites triqueter, Con. (c)
26. Nuculites oblongatus, Con. (rr)
27. Pholadella radiata (Con.), Hall. (r)
28. Orthonota (2) parvula, Hall. (rr)
29. Prothyris lanceolata, Hall. (ar)
30. Macrodon Hamiltonie, Hall. (r)
31. Leda diversa, Hall. (rr)
32. Nucula bellistriata (Con.), Hall. (17)
33. Microdon (Cypricardella) tenuistriatus, Hall. — (ar)
34, Modiomorpha concentrica (Con.), Hall. (1r)
35. Modiomorpha mytiloides (Con.), Hall. (1)
36. Modiomorpha subalata (Con.), Hall. (17)
87. Goniophora Hamiltonensis, Hall. ar)
38. Goniophora PUGOSA (Con.), S. A. Miller (2). (1r)
39. Grammysia arcuata (Con.), Hall. (r)
40. Grammysia sp. (r)

41. Leptodesma Pogersi, Wall. (1r)

>
m oO bo

45.

— i
CO <1 &

or
me © © CO AT & ao HF Oo DK &

aro
go bo

14.

21.

ProssER—HAMILTON AND CHEMUNG

. Pterinopecten Vertumnus, Hall.
. Orthoceras sp. (fragment).
. Platyceras carinatum, Hall.

Phacops rana (Green), Hall.

3. Dalmanites Boothi (Green), Hall.
. Homalonotus De Kayi (Green), Emi.

. Crinoid stems.

MIDDLE PART OF GLEN.

. Spirifer fimbriatus (Con.), Bill.

. Spirifer granulosus (Con.), Hall and Clarke.
. Spirifer audaculus (Con.), Hall and Clarke.
. Spirifer mucronatus (Con.), Bill.

. Orthis Vanuxemi, Hall.

. Cryptonella planirostra, Hall.

. Tropidoleptus carinatus (Con.), Hall.

. Ambocelia umbonata (Con.), Hall.

. Chonetes carinata (Con.), Hall.

. Chonetes setigera, Hall.

. Athyris spiriferoides (Eaton), Hall.

. Cyrtina Hamiltonensis, Hall.

SERIEs.

(c)
(ir)
(rr)

(c)
(rr)
(rr)
(17)

(¢)
(a)
(rr)
(Cc)
(a)
(rr)
(ar)
QT)
(ar)
(¢)
(c)
(Tr)

Orthothetes Chemungensis (Con.), Hall and Clarke. (7)

Cypricardinia indenta (Con.), Hall.

. Nucula bellistriata (Con.), Hall.
. Modiella pygmea (Con.), Hall.

. Macrodon Hamitltonie, Hall.

. Schizodus appressus (Con.), Hall.
. Nuculites triqueter, Con.

. Goniphora Hamiltonensis, Hall.

Modiomorpha concentrica (Con.), Hall.

. Microdon (Cypricarddla) bellistriatus, Con.
. Microdon (Cypricardella) tenuistriatus, Hall.
. Grammysia constricta, Hall.

. Trilobite (fragments).

. Orthoceras (fragment).

. Crinoid stems (large).

UPPER PART OF GLEN NEAR THE MILL.

. Tropidoleptus cavrinatus (Con.), Hall.

. Crania (internal impression ).

()
QT)
ar)
(ar)
ar)
ar)
QT)

(1)
ar)
(aT)
(rr)
(rr)
(rr)

(r)

(a)
(rr)

107

108 Report OF THE STATE GEOLOGIST.
3. Stropheodonta perplana (Con.), Hall. ()
4. Orthothetes Chemungensis (Con.), Hall and Clarke (¢). (rr)
d. Ambocelia umbonata (Con.), Hall. (c)
6. Spiriter granulosus (Con.), Hall and Clarke. (1)
7. Spirifer mucronatus (Con.), Bill. (7)
8. Spiriter audaculus (Con.), Hall and Clarke. (ir)
9. Productella sp. (ar)
10. Orthis Vanuremt, Hall. (r)
11. Chonetes coronata (Con.), Hall. (7)
12. Chonetes setigera, Hall (2). (c)
13. Lingula sp. (ar)
14. Nucula bellistriata (Con.), Hall. (1)
15. Nueula lirata (Con.), Hall. (ar)
16. Nuculites triqueter, Con. ar)
17. Nuculites oblongatus, Con. (rr)
18. Palwoneilo constricta (Con.), Hall. (1)
19. Palwoneilo emarginata (Con.), Hall. (1r)
20. Microdon (Cypricardella) bellistriatus, Con. (7)
21. Paracyclas tenuis, Hall. (ar)
22. Prothyris lanceolata, Hall. (rr)
23. Leda diversa, Hall. (ar)
24. Orthonota carinata, Con. (ar)
25. Grammysia arcuata (Con.), Hall. (1r)
26. Schizodus appressus (Con.), Hall. qr)
27. Modiomorpha mytiloides (Con.), Hall. (11)
28. Pterinopecten Vertumnus, Hall. (ir)
29. Liopteria sp. (1r)
30. Phacops rana (Green), Hall. (c)
31. Pleurotomaria sp. (rr)
Specimens too imperfect to decide whether P. Jtys, H., or P.
capillarva, Con.
32. Platyceras sp.

xX

VIII F. On the south side of Pleasant brook, less than a mile south-

west of Smyrna village, is a steep hill, the summit of which is approximately
500 feet above the Ontario & Western railroad station, or the shales of A},

EXposet

mill, at

| along the brook below the station. For some distance above the

the upper end of the village, there are only occasional exposures of

rock along the banks of Pleasant brook, while the slope of the hill to the

SECTUNA GE PLEASANT BROOK,
MY WIL WEST OF

SMU RNG.

(4 8 O*e B.)

162.0 AN. Appros.

' orca Sanaatants Ln Quosry, ear Cop 0
495 peel AU. Bose 04 yeaAace ae

5 Coveyed
SALRQBURWELS)

Vine Blue Shoes.

as Arshway F SURA-

Orvenaceous Shales BURAWE
Partly Covered.

205" Y Covered.

| 87' pe 6 e hee Laue s1owe .
1 2 == 8

W Shales And Abundant
Bossils.

Wiosily Covered

a

= = 40 ==0 “Qrew. Abundant Fossils.
26 ER Rart\y Covered
KO WAMU IN Shales.
Below O.FW. AR Srotion, W277’ Cce:

109

Shales Wik Chin Sandslones Aw

110 Report oF THE STATE GEOLOGIST.

south is largely covered by soil. However, on the “ Barber lot,” owned by
William Wilcox, there is a small brook along whose course the rocks are
partly exposed. In the woods at the foot of a cascade about 110 feet above
the top of the shales in Pleasant brook at XVIII A‘ is a fair outcrop of
shales which contain an abundance of fossils. There is a continuous exposure
of twelve feet of these shales which in both faunal and lithologic characters
are similar to the Moscow shales of western central New York. Only a few
minutes were spent there in collecting, but in that time nineteen species were
obtained, all of which, with the exception of Chonetes mucronata, Hall, Cryp-
tonella (Eunella) Linckleni, Hall, and Liopteria DeKayi, Hall, occur in the
Moscow shales in the vicinity of Moscow and Livonia, Livingston county,
New York,’ which is the typical region for this subdivision of the Hamilton

formation. ‘The complete list of species is as follows:

1. Spirifer mucronatus (Con.), Bill. (a)
2. Spirifer granulosus (Con.), Hall and Clarke. (rr)
3. Spirifer audaculus (Con.), Hall and Clarke. (7)
4. Spirifer Tullius, Hall. (r)
5. Vitulina pustulosa, Hall. (aa)
6. Tropidoleptus carinatus (Con.), Hall. (c)
7. Athyris spiriferoides (Katon), Hall. (rr)
8. Chonetes coronata (Con.), Hall. (rr)
9. Chonetes mucronata, Hall. (rr)
10. Cryptonella (Funella), ct. Linckleni, Hall. (r)
11. Stropheodonta perplana (Con.), Hall. (ar)
12. Nuculites triqueter (Con.). (ar
13. Paleoneilo constricta (Con.), Hall. (rr)
14. Nuecula bellistriata (Con.), Hall. (rT)
15. Microdon (Cypricardella) tenuistriatus, Hall. (rr)

16. Goniophora, ct. Hamiltonensis, Hall, and carinata (Con.), Hall. (rr)
The concentric plications are coarse and apparently nearer to

to those of G. carinata than G. Hamiltonensis, but the strati-
graphic position of the former is given as higher in the Ithace

group at Oneonta.

17. Liopteria DeKay?, Hall. (rr)
18. Phacops rana (Green), Hall. (1)
19. Dalmanites (Cryphaus) Boothi (Green), Hall. (c)

1 See localities mentioned in the distribution of the species in the volumes on the Paleontology of New York, and especially
lists of fossils from the Moscow shales of the Livonia salt shaft by J. M. Clarke/Thirteenth Annual Report State Geologist [N. Y.],
pp. 134-145).

ProssER—Hamitron AND CHEMUNG SERIEs. see

XVIIT ZB. Immediately above the Hamilton shales which have just
been described, is an argillaceous limestone eighteen feet in thickness forming
a cascade in the run. In places the limestone is quite shaly and very
siliceous, while other portions of the exposure are strongly caleareous.
An analysis by Mr. John B. Anderson of a sample from one of the calcareous

_ layers gave the following result :

INGE G7 see Sh no 06 bo lice 7.85 per cent.
Siete: 5 bed Glee uc 0r0ub 1S DLC ae aCe “SSO ts) or
aaw Omen Mo ete ate ye MR pe Ks oaks Ol dec eee” —*
IIS Oleh, 9 5: VOR aaa 4.28. * ee
Potale <0. 6 ahs che ices See OZ49 = a

This is the Tully limestone. It weathers in a manner similar to the
outcrops farther up Pleasant brook above Upperville, and in the hills near
De Ruyter. This outcrop of the Tully limestone is about two miles southeast
of its previously farthest eastern known exposure, which is on the hillside a
short distance below Upperville, Smyrna township.’

XVIIT B*. Above the limestone for twenty feet in the brook, there
are no outcrops and then grey to bluish, arenaceous unfossiliferous shales
appear. ‘There is scarcely any trace of the black Genesee slates along the
brook, even as loose pieces. However, that part of the brook without out-
crops, between the arenaceous shales above and the limestone below, is the
place for the Genesee slate, consequently it may be represented at this locality
and be covered by soil. The blue arenaceous shales are fairly exposed along
the upper part of the brook on the highway and in the field above, with a
thickness of 140 feet. Then for 130 feet higher, forming the upper portion
of the slope, there are no outcrops, all the rocks being covered by the soil.
The fine blue shales are well exposed for some distance along the highway,
on the slope, but a hasty search revealed no fossils. Part of the shales are
very smooth and split into thin pieces, and these are well shown in a small
brook by the side of the highway on the opposite side of the hill. At this
place no fossils were found. |

These bluish, unfossiliferous shales, at least 140 feet in thickness, belong

Science, Vol. XXXVI, p. 210.) Also by Prof. S. G. Williams in the Sixth Annual Report State Geologist |New York], p. 18.

The calcareous strata in eastern Pennsylvania which the Pennsylvania geologists correlated with the Tully limestone of New
York (see Pennsylvania Geological Survey, Summary Description Geology Pennsylvania, Vol. II, 1892, p. 1°13, with map of area
on p. 1314), has been shown by the writer to belong considerably lower in the Hamilton formation. (See Bulletin United States
Geological Survey, No. 120, 1894, pp. 7, 72.)

112 Report OF THE STATE GEOLOGIST.

the region of Ithaca, N.Y. The picture of Taughannock falls gives an excellent
idea of the Lower Portage of the Cayuga lake region. Estimating from other
sections in the Chenango and Unadilla valleys, we may safely refer to the
Portage, the 180 feet of overlying covered rocks of this station, which would
give a thickness of at least 270 feet for the lower Portage near Smyrna.
Vanuxem, in 1840, proposed the name “Sherburne flagstone” for this forma-
tion, the typical locality beg near Sherburne, Chenango county, and
described it as composed of “stones * * * of various grades of thickness,
alternating with greenish or olive-colored shales; Fucoids resembling the
stems of plants are frequent in this rock, and also fragments of plants like the
grasses. The flagstone mass extends from Cayuga lake through the district ”
[Third Geological district, which extended from Cayuga lake eastward to
Delaware and Schoharie counties|'. In the final report on the Third District
Vanuxem referred the Sherburne flagstones and shales to the Portage group.’

After considering the differences in lithology and fauna between the
rocks constituting the Portage formation of western New York and the
synchronous formations of eastern New York, it seems advisable to revive
Vanuxem’s name of Sherburne sandstones as the name of a formation.
If we study the sections of the Portage formation in different parts of
the State, we will find that in western New York, along the Genesee
river, Professor Hall made the following subdivisions of the formation in
ascending order: Cashaqua shale, Gardeau shale and Portage sandstones? In
Ontario county, along Canandaigua lake, Professor J. M. Clarke divided this
formation into the Naples shales and Portage sandstones, regarding the Naples
shales as representing the Cashaqua and Gardeau shales of the Genesee valley.
For the outcrops along the meridian of Cayuga lake Professor H. 8S. Williams
has used the names Lower Portage, Ithaca group and Upper Portage.’ In the
Chenango valley at the base are Vanuxem’s Sherburne flagstones, which are
equivalent to the Lower Portage of the Cayuga lake region, and therefore
represent only a part of the Portage formation; next above is the Ithaca
group, capped by the Oneonta sandstone. The evidence seems to show that
at least all of the rocks referred to the three formations Just mentioned for the
Chenango valley are represented in western New York by the Portage forma-

tion, Since in the Chenango valley and eastward, the rocks which are

! Fourth Avuual Report, Third Geological District (Assembly Document No. 50, 1840), p. 381.
* Geology of New York, Part III., 1842, p. 172.
3 Geology of New York, Part IV., pp. 226-228.
Bulletin United States Geological Survey, No. 16, p. 36 and p. 67.
5 Bulletin United States Geological Survey, No. 3, p. 29, and Transactions American Institute of Mining Engineers, Vol. XVI.,
p. 945.

PLATE |

TAUGHANNOCK FALLS, CAYUGA LAKE.
LOWER PORTAGE WITH GENESEE SHALE IN THE LOWER PART OF THE CLIFF

Mo a

ProssER—HAMILTON AND CHEMUNG SERIES. 113»

synchronous with those of the Portage formation in western New York,
differ so strikingly from the Portage in faunal and lithologic characters,
there would be an advantage in classifying them in such a way as to make
them readily recognizable in the eastern part of the State. The name Oneonta
formation is in general use for the upper part ; Ithaca formation to some extent
for the middle portion; and if Sherburne formation be apphed to the lower
division, there will then be a complete series of formation names for these
terranes, which may be readily followed and mapped half way across New
York. Since the Sherburne formation may easily be followed from Sherburne
to Ithaca, it is proposed that these rocks at the head of Cayuga lake near
Ithaca be called the Sherburne formation.

In this connection it is well to recall the fact that Conrad, in 1841, pro-
posed Sherburne group as the name of a formation’, for shales found near
Smyrna and other localities? The fossils described by Conrad from the Sher-
burne group are Hamilton species, and this zone was referred correctly by
Vanuxem to the Hamilton formation in his final report of 1842.3

As the rocks to which Conrad applied the name, “Sherburne group,”
belong in the upper part of the Hamilton formation, there is little probability
that there will ever be occasion to restore the name, and, furthermore
Vanuxem’s name “Sherburne flagstones” antedates Conrad’s by fully one
year, so that, according to the law of priority, Conrad’s name would be lost.

XVIII 5. Near the top of the hill, at an approximate altitude of
1,620 feet A. T., is a small excavation exposing two feet of shaly sandstones.
The rock is bluish grey in color, and contains some fossils, especially Spiro
phyton, which occurs abundantly. The following species were collected at
this place :

1. Cyrtina Hamiltonensis, Hall. (a)
2. Spirifer mucronatus (Con.), Bill. (c)
3. Spirifer mesacostalis, Hall. (ar)

Specimens in the form of casts which show clearly the median
septum in the sinus of the ventral valve.
. Spirifer audaculus (Con.), Hall and Clarke. (1)
Spirifer, sp. (Tr)

Ot ie

Fragments of external moulds which show impressions of
pustules. The specimens do not have the normal form of S. granu-
losus; ct. S. fimbriatus (2).

1 Fifth Annual Report Pa!aeontologist, State of New York (Assembly Document No. 150, 1841, p. 31).

® Ibid., see lists of fossils on pp. 50-55 for the localities.

3 Geology of New York, Part III., p. 150. The same correlation appears in Professor Hall’s Final Report of 1843 (Geology of
New York, Part IV., p. 184)

114 Report oF THE State GEOLOGIST,

6. Liorhynchus mesacostalis, Hall. (c)
7. Productella cf. speciosa, Hall. Fragment. — (r)
8. Leptodesma Rogersi, Hall. (rr)
9. Aulopora, sp. (rr)
10. Crinoid stems and segments. (r)
11. Spirophyton, sp. (rT)

12. Microdon (Cypricardella) gregarius, Hall. (rr)
Possibly this specimen is not from this locality as the rock is

hithologically somewhat different.

13. Spirifer finbriatus (Con.), Bill. (2) (r)
14. Atrypa reticularis (Lin.), Dalm. (ar)
15. Chonetes setigera, Hall. (rr)
16. Ambocelia umbonata (Con.), Hall. (r)
17. Phacops rana (Green), Hall. (rr)

This exposure of fossiliferous rocks is regarded by the writer 4s con-
taining the early species of the Ithaca epoch of the Chenango valley region.
There is no question that on the same hillside about 288 feet lower than
this fossiliferous shaly sandstone, is the top of the Tully limestone, while the
intervening rocks, as far as exposed, are thin bluish shales in which fossils are
very rare; shales that agree in all respects with those of the lower Portage
or Sherburne formation of central New York. Near Ithaca, from the base
of the lowest rocks referred to the Ithaca group down to the top of the
Genesee shales is 250 feet, which is nearly the thickness of the Sherburne for-
mation in the Chenango valley. This section with others near Smyrna and
Sherburne clearly show that the fossiliferous beds twelve miles farther south
near Norwich and extending along the river valley to Oxford, are not in the
Hamilton formation, but are of later date.

The accompanying picture of a portion of the Fall Creek gorge at
Ithaca, gives an excellent idea of the lithologic characters of the formation
at its typical locality.

XVITT A*. Along the bed of Pleasant brook, about one and three-
quarter miles above Smyrna village, and three-fourths of a mile below Upper-
ville are excellent exposures of coarse, arenaceous shales which contain fossils
in abundance.

Tropidoleptus carinatus (Con.), Hall, is particularly plentiful and there
are many specimens of large Lamellibranchs. The species are those of the

Hamilton formation, as will be seen from the following list :

J = sy
‘
é
4
’
f
‘
if
.
* ; -
—— _

pty
£
,
,

1
i

‘ee

aoe
&
‘ ¥

>

PLATE II

Se.

Naa BECK CR i

TRIPHAMMER ANO FLUME FALLS, FALL CREEK, |THACA,
UPPER PART OF THE ITHACA GROUP,

=

bo

ProssER—HamiIrton AND CurEmMuNG SERIEs.

. Tropidoleptus carinatus (Con.), Hall.
. Chonetes coronata (Con.), Hall.

. Chonetes mucronata, Hall.

. Spirifer granulosus (Con.), Hall and Clarke.

. Spirifer audaculus (Con.), Hall and Clarke (?).

Internal impressions.

. Spirifer mucronatus (Con.), Bill.

. Phynchonella, sp.

. Orthis, sp.

. Productella, sp.

. An impression of a Zerebratuloid.

. Ambocelia wmbonata (Con.), Hall:
. Athyris (Spirigera) spiriferoides (Eaton), Hall.
. Cyrtina Hamiltonensis, Hall.
. Orthothetes Chemungensis (Con.), Hall and Clarke.
. Orbiculoidea, sp.
External impression of the dorsal valve.
. Nucula bellistriata (Con.), Hall.

. Nuculites oblongatus, Con.

. Nuculites triqueter, Con.

. Leda rostellata (Con.), Hall.

. Leda diversa, Hall.

. Paleoneilo constricta (Con.), Hall.

. Paleoneilo muta, Hall.

. Paleoneilo emarginata (Con.), Hall.

. Paleoneilo tenwistriata, Hall.

. Modiella pygmea (Con.), Hall.

. Microdon ( Cypricardella) bellistriatus, Con.
. Paracyclas tenuis, Hall.

. Modiomorpha mytiloides (Con.), Hall.

. Cimitaria, sp.

. Grammysia arcuata (Con.), Hall.

. Grammysia obsoleta, Hall (?).

Internal impressions poorly preserved.
. Schizodus appressus (Con.), Hall.

. Goniophora rugosa (Con.), S. A. Miller.

. Phthonia cylindrica, Hall.

(a)
(c)
(rr)
(a)
(r)

(ar)

. Stropheodonta, sp. (part of an internal impression). (rr)

(Tr)
(rr)
(rr)
(1r)
(1r)
(1r)
(rr)
(rr)
(rr)

(r)
(rr)

(r)
(rr)
(rr)

(c)
(rr)
(ir)
(rr)
(rr)
(rr)
(1r)
(rr)
(7r)
(rr)
(rr)

(r)
(rr)
(11)

(3 5)

116 Report OF THE STATE GEOLOGIST.

36. Mytilarca (Plethomytilus) oviformis (Con.) Hall. (1)

37. Liopteria Bigsbyi, Hall (?). (1)
38. Phacops rana (Green), Hall. (r)
39. Pleurotomaria capillaria, Con. (r)
40. Lellerophon, sp. (rr)
41. Orthoceras, sp. fragments of two species). (1)

2. Coleolus, sp. 1
42. Coleolus, sy

‘ 3) Bees 7 ay =; = 5
43. Crinoid stems, large. (c)

NX VIIT G'. The hill on the south side of Pleasant brook between
Smyrna and Upperville, is steep and mostly wooded. Not far below Upper-
ville, a small run enters Pleasant brook from the south and the rocks are
quite well exposed along its course. At the mouth of the run are shales
similar to those of XVIII C?, containing similar fossils. These shales extend
up the hillside for some distance and are about 147 feet above the level of
the brook which, at thé mouth of the run, is approximately 1,222 feet A. T.,
and contain numerous fossils, Zyopidoleptus carinatus (Con.), Hall, being
especialiy abundant. A hasty search afforded the following species :

1. Tropidoleptus carinatus (Con.), Hall. (a)
2. Spirifer mucronatus (Con.), Bull. (17)
3. Spirifer granulosus (Con.), Hall and Clarke,
or S. audaculus (Con.), Hall and Clarke. (Tr)
Specimen too imperfect for specific identification.
4. Liorhynchus multicostus, Wall. (7)
The lateral plications are very faint.
5. Orthis Vanuwemi, Hall. (rr)
6. Palwoneilo emarginata (Con.), Hall. (ar)
7. Nucula lirata (Con.), Hall. () ar)
A. broken specimen.
8. (2) Schizodus, sp., badty broken specimen. (rr)
9. Crania, sp. very poorly preserved. (rr)
10. Phacops vrana (Green), Hall. (ar)

AVITT G*. On top of these Hamilton shales, 147 feet above the level
of Pleasant brook, is an arenaceous limestone forming the top of the second
cascade in the run. The stratum is composed of three layers as it crosses the
stream, the lowest, ten inches in thickness, containing quite a large percentage
of sand, the upper layer being the purest limestone. A little higher are
rather coarse, arenaceous blue shales, and then the rocks are covered for about
ten feet. At this point is the third cascade in the stream, at the base of which

Prosser—Hamitton anp Cuemune Serres. 117

is an impure limestone, then calcareous shales, and at the top of the cascade
are two layers of impure limestone, separated by a shaly parting, the upper

SHUTTING BELOD UPPER OY
SOUTH SLE OE PLEQASAAT BROWOK
ave, G,)
1524 ON, Approx.

Biue Shales.
SWERBURWE,

Covered,

%
=14 Coveye ‘ 28° Thick.
OPN Ereres fa TULL Limestone
Second Coscade Woyinon,27].

Eivst Coscade WOATUTOKY,

Carthy Covered.

Level VE Ricasant Crook. Onyyror LLY Ol,

layer being six inches thick. Resting on this upper limestone are about two
feet of calcareous, shaly layers, the distance from the foot of the cascade to its
top being fourteen feet. From the base of the lowest calcareous stratum to

118 Report oF THE SratE GEOLOGIST.

the top of these calcareous shales is twenty-seven feet, which mass of rock the
writer regards as belonging to the same horizon as the Tully limestone of
western central New York. This outcrop was first described in 1887 and
was the farthest east that the Tully had been traced! until the exposure
near Smyrna village was discovered, which is described in the present paper.
From my observations on the eastern outcrops of the Tully limestone, I
ascribe its disappearance to a gradual loss of the calcareous material which is
replaced by that of the arenaceous and argillaceous sediments, causing the
rock to present a decidedly different lithologic appearance. This is sub-
stantially the explanation advanced by Professors 8S. G. Williams” and Henry
S. Williams.*

NXVIIT G. For a short distance above the caleareous shales the rocks
are covered, but where the stream forks black fissile shale begins and about
ten feet are shown. For forty feet above the black shales the rocks are mostly
hidden, but at this point are thin sandstones one-quarter to one-half inch in
thickness, with an occasional layer of black shale between them. Fossils
were not found in these black, argillaceous shales, which are regarded as
belonging to the Genesee slate. As a portion of the rocks is concealed, it is
difficult to give their thickness, but from a study of the exposures a little
northwest of this locality, it seems probable that they have a thickness of
twenty feet or more, perhaps of forty feet, as stated by Professor 8. G.
Williams.‘

XVIII G4. Just above the thin sandstones of the run already described
are thicker sandstones, while the shales change to a blue or olive color; on
their upper surface are frequent irregular markings, perhaps partly due to
Fucoids, but mainly to mud markings produced by mechanical causes.
Above the highway the rocks are mainly blue, smooth shales, which weather
to an olive color and split into very thin pieces. In these fine shales no fossils
were found. But not far from the run above described another crosses the
highway, the first one below Upperville, and in this, about thirty feet above
the highway, is the Wilcox quarry, which has been worked for building
stone, the heaviest layer being nineteen inches thick. There is an occasional
thin flag layer and the sandstones alternate with shales. Fossils are rare,

¢ found in an hour’s search, as the list

only a very few specimens being

shows:

1See Prosser, Proceedings American Association Advancement of Science, Vol. XXXVI, p. 210; and S. G. Williams, Sixth
Annual Report State Geologist [New York], p. 18.

2 Sixth Annual Report State Geologist [New York], 1887, p. 18.

4 Bulletin Geological Society of America, Vol I, 1+90, p. 490.

4Sixth Annual Report State Geologist [New York], p. 18.

ProssER—HamILtoN AND CHEMUNG SERIES. 119

1. Lunulicardium fragile, Hall. (vr)

2. Liopteria sp. (rr)

3. Crinoid stems.

A single specimen of Liorhynchus mesacostalis, Hall, was found, but it
was on a loose piece of stone in the quarry, and may have come from farther
up the hillside. On the highway below the quarry are black, argillaceous
shales of the Genesee, and in the run below the road is the Tully limestone.
The thin sandstones which contain an occasional fossil, and the blue shales
that weather to an olive color, belong to the Sherburne formation.

The clear stratigraphic succession of the rocks forming this section ; the
very fossiliferous shales with abundant Hamilton fossils in the lower part of
the run, belonging in the Hamilton formation; followed by twenty-seven feet
of calcareous layers, part of which are impure massive limestones, referred to
the Tully; succeeded by a black, argillaceous shale similar in all its litho-
logic characters to the Genesee; capped finally by thin sandstones and blue
or olive shales, called the Sherburne, and which contain a few fossils, seem to
prove the correlation offered by the writer for the rocks of this region. The
stratigraphic order of the rocks just described is shown diagrammatically in
the accompanying section.

AX VIIT A®, Gorge and falls in Pleasant brook at Upperville. The water
falls over about fifteen feet of coarse, blue, arenaceous shales, in which fossils
are common, particularly Spirifer granulosus (Con.), Hall and Clarke, and
some large Lamellibranchs. Some of the shales which contain many shells are
somewhat calcareous, and the outcrop extends along the bed and sides of the
brook for some distance below the falls. The rocks belong to the Hamilton
formation, and the following species were collected :

1. Spirifer audaculus (Con.), Hall and Clarke. — (¢)
2. Spiriter granulosus (Con.), Hall and Clarke. (c¢)

3. Spiriter mucronatus (Con.), Bill. (rr)
4. Cyrtina Hamiltonensis, Hall. (c)
5. Orthis Vanuxemi, Hall. (r)
6. Chonetes mucronata, Hall. (rr)
7. Palewoneilo fecunda, Hall. (2) (rr)
8. Paleoneilo emarginata (Con.), Hall. (ar)
9. Modiomorpha concentrica (Con.), Hall. (ar)
10. Grammysia arcuata (Con.), Hall. (17)
11. Phacops rana (Green), Hall. (1)

12. Bellerophon crenistria, Hall. (?) (1r)

120 Report OF THE STATE GEOLOGIST.

13. Orthoceras (fragment ). (17)
14. Ooleolus tenuicinctum, Hall. (7r)

XVIII A‘. Exposures in Pleasant brook below Card’s mill, one mile
above Upperville. The rocks are blue shales that split into fine, smooth
fragments, alternating with calcareous layers which contain fossils in abund-
ance and form layers termed “firestones.” Such a calcareous layer six inches
in thickness is exposed in the bed of the brook under the highway bridge and
contains a large number of fossils, as Spirifer mucronatus (Con.), Bill., and
other species. In the shales above the calcareous stratum just mentioned are
large numbers of Liorhynchus multicostus, Hall, which is the most common
fossil at this locality. This exposure is about seventy-five feet above the
falls at Upperville, and is in the Hamilton formation. The following species

were collected :

1. Liorhynchus multicostus, Hall. (aa)
2. Orthothetes Chemungensis (Con.), Hall and Clarke. ar)
3. Athyris (Spirigera) spiriferoides (Eaton), Hall. (7)
4. Spirifer consobrinus, D’Orbigny—ziczac, Hall. (rr)
5. Spiriter granulosus (Con,), Hall and Clarke. (17)
(Imperfect specimen. )
6. Spirifer mucronatus (Con.), Bill. (rr)
7. Spirifer audaculus (Con.), Hall and Clarke. (1r)
8. Atrypa reticularis (Lin.), Dalm. — (rr)
9. Orthis Vanuxemi, Hall. (?) (1)
10. Ambocalia umbonata (Con.), Hall. (1)
11. Stropheodonta, sp. (very imperfect specimen). (ir)
12. Tropidoleptus carinatus (Con.), Hall. (c)
13. Chonetes scitula, Hall. (c)
14. Chonetes setigera, Hall. (7)
15. Terebratuloid shell too imperfect to identify generically. (rr)
16. Orbiculoidea, sp. ct. with O. Seneca, Hall. (rr)
17. Nucula bellistriata (Con.), Hall. ar)
18. Nucula lirata (Con.), Hall. (2) (ir)
19. Palwoneilo constricta (Con.), Hall. (rr)
20. Palwoneilo emarginata (Con.), Hall. (rr)
21. Palwoneilo muta, Hall. (rr)
22. Modiella pygmwa (Con.), Hall. (ar)
23. Tellinopsis subemarginata (Con.), Hall. (Vr)

24. Modiomorpha subalata (Con.), Hall. (ar)

ProssER—HamILron AND CHEMUNG SERIES. 121

25. Modiomorpha mytiloides (Con.), Hall. (rr)
26. Modiomorpha concentrica (Con.), Hall. (rr)
27. Phacops rana (Green), Hall. (rr)
98. Trilobite, sp. (fragment). (11)
29. Orthoceras, sp. (fragment). (17)
30. Platyceras (too imperfect to identify specifically). (ir)
31. Bellerophon, sp. (two very imperfect specimens). ar)

XVITT A®. On Pleasant brook just above the upper highway bridge,
five and one-half miles above Smyrna village, on the Gilbert Tuttle farm, is
an exposure of shales and limestone. Below the limestone are one and one-
half feet of black, argillaceous shales that are quite fossiliferous, containing
numerous specimens of typical Spirifer mucronatus (Con.), Bill, Vitulina
pustulosa, Hall, and other Hamilton fossils. This outcrop is some 275 feet
by the barometer above the New York, Ontario and Western railroad
station in Smyrna, or approximately 1,400 feet A. T., and is at the top of the
Hamilton formation. The following species were collected :

1. Spirifer mucronatus (Con.), Bill. (a)
2. Vitulina pustulosa, Hall. (a)
3. Tropidoleptus carinatus (Con.), Hall. (ir)
4. Chonetes, sp., probably C. setigera, Hall. (rr)
5. Modiella pygmoaa (Con.), Hall. (Vr)
6. sVuculites oblongatus (Con.). (1r)
7. Orthonota undulata (Con.). (17r)
8. Palwoneilo emarginata (Con.), Hall. (rr)
9. Dalmanites Boothi (Green), Hall. (7)
10. Lellerophon, sp. (rr)
11. Internal impression of a large Orthoceras from a loose slab of sand-

stone in the creek.

XVIIf A®. On top of the shales are three and a half feet of somewhat
impure limestone, separating into two or three layers, the upper being the
purer. Above the limestone, part of which is dark in color and strongly
calcareous, with the lithologic characters of the Tully, the rocks are covered
by soil. A little farther up the brook is another outcrop of rather impure
limestone five feet in thickness, which is apparently higher than the former.
It seems probable that there are fully ten feet of the impure limestone at
this loeality, and the actual thickness is no doubt somewhat greater, but is

obscured by the soil.!. So far no fossils have been found in this limestone

1 Professor S. G. Williams, in describing this locality, stated the indications were that ‘‘the limestone is at least fifteen feet
thick,’’ (Sixth Annual Report State Geologist |New York], p. 18).

122 Report oF THE STATE GEOLOGIST.

along Pleasant brook, but none of the outcrops are favorable for collecting,
and it is very likely if the rocks were opened to any extent that fossils would
be found.

This is supposed to be the most eastern locality of the Tully limestone
observed by Vanuxem, for he said, in describing the localities of this rock:
“The first point going west is on the turnpike from Sherburne to De Ruyter,
about eight miles from the former village. It appears in a low side hill,
forming the bank of the creek where the road crosses it. About four layers
are exposed, ranging by the side of the creek.”' Again, in describing the
geology of Chenango county, Vanuxem wrote: “The Tully limestone was
seen in but one locality at the northwestern part of Smyrna, on the road to
De Ruyter village, where the road crosses the west branch of the Chenango.” ?

AXVIIT A*. In Pleasant brook and along its bank, about one-half mile
above the first outcrop of Tully limestone, are black argillaceous shales, which
form a bluff fifteen feet in height on the south bank of the creek. The shales
weather to very thin pieces, and in lithologic characters resemble closely the
Genesee slates as exposed on Cayuga and the other lakes of wesiern central
New York. The shale is so black that some years ago an excavation was
made in the hope of finding coal. No fossils were found by me. Between
the Tully limestone and the lowest layers of the shale on the creek the rocks
are covered for some distance, the shales being about thirty-five feet above
the last outcrop of the limestone; then there are at least fifteen fect of black
shales, and next, following a small stream up the hill to the south of Pleasant
brook for about twenty-five feet, the rocks are covered and sandstones and
shales occur.

XVIII A®. The sandstones, which are of a dark gray color, weathering
to a rather brownish tint, alternate with greenish shales. Fifty feet of the
shales and sandstones occur along the run and reach the brow of the hill.
Along the upper part of Pleasant brook the hills are much lower than in the
vicinity of Smyrna village. The thin sandstones of these rocks show on the
upper surfaces numerous specimens of /ucoides graphica, Van., and in general
lithologic characters are similar to the shales and sandstones constituting
the Sherburne formation in Cortland and Tompkins counties. The base of
these Sherburne rocks is about seventy-five feet above the top of the Tully
limestone, or barometrically 360 feet above the New York, Ontario and
Western railroad station at Smyrna, making the altitude approximately 1,485
feet A. T.

1 Geology of New York, Part III., p. 164.
2 Thid., p. 292.

ProssER—HaAMILTON AND CHEMUNG SERIES. 123

These three sections along Pleasant brook and up the hill to the south
through the central part of Smyrna township are regarded by the writer as
very important in deciding where the line of separation between the Hamilton
and Chemung series should be drawn. It is nearly, if not quite, the most
eastern locality at which the lithologic characters of the Tully limestone and
Genesee shale agree closely with those of their typical localities in the more
western portions of New York. Above the black shale occur thin sandstones
and olive to bluish shales which agree well lithologically with the lower part
of the Sherburne formation, as shown along Cayuga lake, while on the top of
the high hills oecur sandstones and shales containing fossils which compose

the lowest fauna of the Ithaca group, as developed in Chenango county.

Sherburne.

The next township to the east of Smyrna is Sherburne, which also
belongs to the northern tier of townships in Chenango county, and as the
Chenango river flows from north to south entirely across the western half, it
forms one of the townships of the Chenango river valley. To the north is
Hamilton township, on the east is Columbus which extends east to the
Unadilla river.

- The valley of the Chenango river in central New York is noted for its
beauty. Rather narrow in general, from one-half to two miles in width, there
are steep hills rising on one and usually both sides of the valley. In places
the hills are so steep that numerous exposures of the rocks along their sides
are seen, but usually the best sections are afforded by the small runs and
brooks that have trenched more or less deeply the hills that bound the river
valley. These hills extend from the northern line of Chenango county for
forty-five miles to the southwest until the Susquehanna is reached near Bing-
hamton.

These sections occur in the Middle and Upper Devonian of southern
central New York. In order to bring out clearly the character and succes-
sion of these formations, a series of sections with their fossils will now be
described approximately in the order of their occurrence from Sherburne on
the north to the vicinity of Binghamton on the south.

AIX A*. To the southeast of Smyrna, between the New York,
Ontario and Western and the Delaware, Lackawanna and Western railroads,
is a hill on whose eastern side, about two miles southwest of Sherburne
village, and just west of the turn in the highway approaching the village, 1s
an old quarry of shaly sandstone. The back of the quarry shows a ledge

124 Report oF THE Strate GEOLOGIST.

eleven feet thick, in which Hamilton fossils are common, and from which the

following species were obtained :

1. Spirifer mucronatus (Con.), Bill. (a)
2. Tropidoleptus carinatus (Con.), Hall. (1r)
3. Chonetes scitula, Hall. (c)
4. Athyris spiriferoides (Eaton), Hall (?). (ar)
Imperfectly preserved internal impression.
5. Grammysia (Sphenomya) cuneata, Hall. (1r)
6. Microdon ( Cypricardella) tenuistriatus, Hall. ar)
7. Tellinopsis subemarginata (Con.), Hall. (1r)
8. Actinopteria decussata, Hall. (ar)
9. Orthoceras, sp. (poorly preserved fragment). (ar)

10. Dalmanites (Crypheus) Boothi (Green), Hall. (ar)

The Hamilton arenaceous shales, with plenty of fossils, extend at least
sixty feet higher than the quarry, where an outcrop was found which is
barometrically 175 feet above the Delaware, Lackawanna and Western rail-
road station at Sherburne, or approximately 1,220 feet A. T.

ATX A*, Above the Hamilton outcrop just mentioned the rocks are
covered for about sixty-three feet, when another old quarry is reached, in
which there are thin, bluish sandstones alternating with thin, bluish, fissile,
argillaceous shales, and this outcrop may be followed for some distance along
the side of the hill to the north. No fossils were found except fucoidal mark-
ings similar to H’ucoides graphica, Van. The quarry is barometrically 238 feet
above the Delaware, Lackawanna and Western railroad station at Sherburne.
The rocks belong to the Sherburne formation, and the upper portion of this
hill has been so indicated on the accompanying geologic map.

ALIX +". Inthe northern part of Sherburne township, about two and
one-half miles northeast of the village, on the Powers farm, two excavations
were made some years ago in search of coal, and the place is known locally as
the “coal mine.” The rocks are mostly thin, fissile, black, argillaceous shales,
containing abundant Hamilton fossils. Some of the layers are composed very
largely of Spirifer mucronatus (Con.), Bill, and Tropidoleptus carinatus (Con.),
Hall. The most abundant species are Spirifer mucronatus (Con.), Bill,
Tropidoleptus carinatus (Con.), Hall, and Ambocelia umbonata (Con.), Hall,
and the rocks belong in the upper part of the Hamilton formation, probably
the zone termed in western New York, the Moscow shale. Barometrically the
locality is 266 feet above the Sherburne railroad station, or approximately
1,308 feet A. T.

WD BAWH STLMIM| COVE OE
SVEABURL
heros.

\36\ QN. yprax,

Shales Wilk, LDRAYTOAUS

————
—%

525 =F WMESACOUSTOUS. WTOC
Rasily Govesea

e SWERBOUAITE, Vragsi ones,

SSS
SaaS
ee
[ee eee

443"

Coveyed.
SHERBURIE

5 Swan Quaassy,
oie Wamrfor Lamellesanehs.
240 Tor 04% Lowes Resesvors Vom
oy OW Worrisuille.

eee AY Consse Shales Qnd Sondstones
a SPARLEER QRANULISAS.
S|, Coorse Blue Sholes With

B Thin Sonadsiones

Bok 05 Reaiova Kal\s

j33:

VYOMUMLTN

Se OB\we Shales |

62’
. & Blue Shales Wik
32 Noundant Fossils.
0’ Covesead

RRL gue bn Sherburne,

1042 ON,

125

s
126 Report oF THE SraTE GEOLOGIST.

XIX #*. On the western side of the small valley formed by Herrington
brook and to the northwest of the “coal mine” is a steep hill 200 feet higher.
Near the top of the hill is Mulligan’s quarry, from which bluish, fine-grained,
thin flagstones are produced. Most of the layers are only from one-half to
two inches thick, but the workmen claim that if well bedded they do not
_ break easily, and the flags have been used to some extent in the village for
sidewalks. Above the flags in the quarry are rather coarse, irregular shales,
which contain fossils ; Liorhynchus mesacostalis, Hall, and Spirifer are common.
This quarry is barometrically about 455 feet above the railroad station in
Sherburne, or approximately 1,500 feet A. T., and is considered as belonging
to the lower part of the Ithaca group. The hill is composed of the Sherburne
and Ithaca formations, and has been so represented on the geologic map.

XTX F'. In the eastern part of Sherburne village is a stream known as
Mad brook, which has rocky banks for a mile or more. At the head of the
glen is Sherburne or Rexford falls, a local summer resort and picnic ground.
The rocks along the side of the brook contain numerous fossils, making an
excellent locality for collecting species found in the upper part of the Hamil-
ton formation. The lowest exposures of rocks in Mad brook are in the edge
of the village, only thirty-two feet, by the level, above the railroad, or with
an altitude of 1,074 feet A. T. They are thin, blue shales, that split very
finely, contain numerous fossils and some calcareous layers, composed princi-

pally of fossils. The observed fauna is as follows:

1. Orthis Vanuaemi, Hall. (c)
2. Athyris (Spirigera) spiriferoides (Katon), Hall. (r)
8. Stropheodonta perplana (Con.), Hall. (r)
4. Stropheodonta inequistriata (Con.), Hall. (a)
5. Spirifer mucronatus (Con.), Bill. (a)
6. Spirifer granulosus (Con.), Hall and Clarke. (rr)
7. Spirifer audaculus (Con.), Hall and Clarke. (rr)
8. Spirifer fimbriatus (Con.), Bill. ar)
9. Orthothetes Chemungensis (Con.), Hall and Clarke. (2r)
10. Chonetes coronata (Con.), Hall. (r)
11. Centronella impressa, Hall. (?) (r)
12. Tropidoleptus carinatus (Con.), Hall. (c)
13. Orbiculoidea sp. (rr)
14. Lingula (portion of a valve). (rr)
15. Nucula bellistriata (Con.), Hall. (rr)

16. Macrodon Hamiltonia, Hall. (c)

-—
~J

bdo wp Ww Ww HW FE
= Ow wore © CO

25.

ACI. s.

PRossER—HAMILTON AND CHEMUNG SERIES.

. Paleoneilo constricta (Con.), Hall. (r)
. Goniophora Hamiltonensis, Hall. (r)
. Microdon (Cypricardella) bellistriatus, Con. (rr)
. Mytilarca (Plethomytilus) oviformis (Con.), Hall. (r)
. (2) Liopteria (very imperfect specimen). (rr)
. Phacops rana (Green), Hall. (r)
. Loxonema delphicola, Hall. (rr)
. Gomphoceras, sp. (ar)

Portion of a Crinoid stem. (rr)

The shales farther east by the side of Mad brook, just above

the highway bridge, are sixty-two feet by level above the railroad. The rocks

are blue, argillaceous (somewhat arenaceous) shales, containing abundant

fossils, generally small forms of lamellibranchs and brachiopods, with an

occasional large lamellibranch and trilobite.

The following species were

collected :

1. Chonetes coronata (Con.), Hall. (aa)

2. Chonetes setigera, Hall. (aa)

3. Chonetes scitula, Hall. (?) (r)

4. Chonetes lepida, Hall. (rr)

5. Spirifer mucronatus (Con.), Bill. (aa)

6. Spirifer granulosus (Con.), Hall and Clarke. (rr)

7. Spiriter fimbriatus (Con.), Bill. (rr)

8. Spiriter Tullius, Hall. (?) (rr)

(A single internal impression of a ventral valve.)

9. Ambocelia wumbonata (Con.), Hall. (r)
10. Athyris spiriferoides (Katon), Hall. ()
11. Orthis Vanuxemi, Hall. (r)
12. Stropheodonta, sp. (internal impression of large valve). (17)
13. Orbiculoidea, sp. (11)
14. Lingula, sp. (1r)

It has the same proportions as L. /igea, H., though slightly larger
15. Lingula, sp. (rr)
A broken specimen resembling 1. comp/lanata, Williams.
16. Nuculites triqueter, Con. (aa)
17. Nuculites oblongatus, Con. (t)
18. Paleoneilo constricta (Con.), Hall. (2)
19. Paleoneilo emarginata (Con.), Hall. (1)
20. Pulwoneilo muta, Hall. (1)

128 Report oF THE STATE GEOLOGIST.

21. Nueula bellistriata (Con.), Hall. (c)
22, Nucula corbuliformis, Hall. (7)
23. Nucula lirata (Con.), Hall. (7)
24. Paracyclas tenuis, Hall. (1r)
25. Schizodus, sp. (2), Gmperfect specimen). (1r)
26. Macrodon Hamiltonie, Hall. (rr)
27. Modiella pygmwa (Con.), Hall. (c)
28. Orthonota (2) parvula, Hall. (r)
29. Orthonota carinata, Con. (7)
30. Orthonota undulata, Con. (2) @)
31. Lunulicardium fragile, Hall (2). (Vr)
32. Cimitaria elongata (Con.), Hall (2). (1)
33. Pholadella radiata (Con.), Hall. (aa)
34. Prothyris lanceolata, Hall. (ar)
35. Grammysia arcuata (Con.), Hall. (c)
36. Grammysia bisulcata (Con.), Hall. (a)
387. Modiomorpha mytiloides (Con.), Hall. (11)
38. Sphenotus solenoides, Hall. (11)
39. Sphenotus truncatus (Con.), Hall (?). (7r)
40. Goniophora, sp. (probably G. Hamiltonensis, H.). (ar)
41. Tellinopsis subemarginata (Con.), Hall. (ar)
42. Cypricardinia indenta (Con.), Hall. (ar)

43. Microdon (Cypricardella) bellistriatus, Con. (fragments). (17)
44. Liopterva, sp. (1)
With poorly preserved specimens it is difficult to make specific

identifications when the species of this genus differ so slightly.

45. Pterinopecten Vertumnus, Hall (4). (c)
ef. P. intermedius, H.
46. Glyptocardia speciosa, Hall. (rr)
47. Dalmanites Boothi (Green), Hall. (c)
48. Phacops rana (Green), Hall. (1)
49. Homalonotus De Kayi (Green), Emm. (ar)
50. Bellerophon Leda, Hall. (1)
51. Bellerophon acutilirata, Hall. (11)
52. Cyrtolites (Cyrtonella), sp. (ar)
53. Pleuwrotomaria capillaria, Con. (1)
54. Loxonema delphicola, Hall. (a)

55. Coleolus tenuicinctum, Hall. (r)

Pross—ER—H amitton AND CHEMUNG SERIES. 129

56. Tentaculites, sp. (a single impression). (rr)
57. Orthoceras, sp. (fragments of two species). (1)
58. Crinoid stems. (1r)

XIX 4°. Sherburne or Rexford falls, one mile east of Sherburne village.
The foot of the falls is 133 feet by level above the railroad, or 1,175 feet A. T.
The shales are coarser than those farther down the brook, quite blue, and
alternate with blue sandstone, some of the strata of which are two feet thick.
In the glen below the falls is a sulphur spring, and the place is well known

locally as a picnic ground. The following species were here collected :

1. Spirifer granulosus (Con.), Hall and Clarke. (1)
2. Spirifer fimbriatus (Con.), Bill. (1’)
3. Spirifer mucronatus (Con.), Bill. (rr)
4. Spirifer Tullius, Hall. (17)
5. Tropidoleptus carinatus (Con.), Hall. (1)
6. Orthis Vanuxemi, Hall (2). (1)
7. Orthothetes Chemungensis (Con.), Hall and Clarke. (rr)
8. Ambocelia umbonata (Con.), Hall. (c)
9. Chonetes coronata (Con.), Hall. (11)
10. Chonetes mucronata, Hall. (rr)
11. Chonetes setigera, Hall. (1r)
12. Chonetes scitula, Hall. (1r)
18. Palwoneilo constricta (Con.), Hall. (rr)

XIX L*. Mad creek, just below the Sherburne reservoir at Harrisville,
one and one-half miles east of Sherburne village. The lower dam at the top
of these shales is about 240 feet above the railroad by surveyor’s leveling,
making the altitude of this locality about 1,282 feet A. T. The rocks are
coarse, arenaceous Hamilton shales, alternating with shaly sandstones, and
characteristic Hamilton fossils are abundant, as for example, Spiriter granu-
losus (Con.), Hall; Zropidoleptus carinatus (Con.), Hall; Spirophyton velum
(Van.), Hall, mingled with some of the larger lamellibranchs. The rocks
form a small fall just below the lower reservoir dam, and at its base finer
shales occur. The coarse, shaly sandstones contain large numbers of per-
fect specimens of the Spirophyton velum (Van.), Hall, making an excellent
locality for collecting specimens of this interesting fossil. The complete list

is as follows:

1. Spirifer granulosus (Con.), Hall. (aa)
2. Spiriter audaculus (Con.), Hall.—=S. medialis, H. (c)
3. Spirifer mucronatus, (Con.), Bill. (c)

i

130 Report or THE Srare GEoLoGIst.

4A. Tropidoleptus CUPLNALUS (Con.), Hall. (: )
5. Cyrtina Hamiltonensis, Hall. (v)
6. Grammysta arcuata, (Con.), Hall. (rr)
7. Grammysia bisulcata (Con.), Hall. (rr)

8. Crinoid segments.
9. Spirophyton velum (Van.), Hall. (c)

ATX 7G. On the south side of the highway and the south branch of
Mad brook, opposite the reservoir, is the Swan quarry, which is only about
ten feet higher than the top of the upper reservoir dam or some 273 feet
above the railroad at the village, or 1,815 feet A. T. At the bottom of the
quarry is a bluish sandstone from one and one-half to two feet thick, which
has been quarried to some extent, capped by about eight feet of rather arena-
ceous shales that contain plenty of small Hamilton lamellibranchs. During

a hasty search the fe lowing species were collected :

lL. Spirifer mucronatus (Con.), Bill. (2)
2. Liorhynchus multicosta, Wall. (aa)
3. Tropidoleptus carinatus (Con.), Hall. (1)
4. Spirifer Tullius, Fall. (rr

. The shell has distinctly the form of this species and near the
front of the valves are apparently traces of striae on the plications.
There are several very small specimens of Sp/rifer which may

possibly belong to this species.

d. Palawonetlo constricta (Con.), Hall. ()
6. Nueula lirata (Con.), Hall. (c)
7. Nucula bealistriata (Con.), Hall. (rr)
8. Nueculites triqueter, Con. (7r)
9, Paleoneilo emarginata (Con.), Hall. (ar)
10. Phthonia cylindrica, Hall. (ar)
11. Modiomorpha mytiloides (Con.), Hall (2). (11)

The striae are of this species but the shape at the anterior end
is nearer that of JZ. concentrica (Con.), Hall.

12. Liopteria DeKayi, Hall (4). (rr)
13. Orthothetes Chem UNGENSTS (Con.), Hall and Clarke,

var. perversd, Hall. ar)
14. Grammysia (Sphenomya) cuneata, Wall. (ar)

Crushed specimen agreeing closely with the description of this

species.

ProssER—Haminton AND CHEMUNG SERIES. 131

XIX BB. Above the Swan quarry is a steep hill with but few outcrops.
On the highway up this hill, at an elevation of 170 feet above the Swan
quarry, is a clear outcrop of the Sherburne flagstones, but these thin sand-
stones appear lower on the highway, and it is probable that the Swan quarry
is near the top of the Hamilton formation.

XIX B. Along a small run on the western side of the highway, near
the brow of the hill, are shales. This outcrop is barometrically 252 feet
above the base of the Swan quarry or approximately 1,567 feet A. T. Fossils
are rare with the exception of Liorhynchus mesacostalis, Hall, fourteen speci-

mens of which were collected. The list is as follows:

1. Liorhynchus mesacostalis, Hall. (a)

2. Chonetes setigera, Hall (2). (7r)
Imperfectly preserved.

3. Nucula corbuliformis, Hall (?). (ar)

Very imperfect specimen.

4. Crinoid segments. (7)

This outcrop probably contains the first of the Ithaca fauna, though it
is lower than its appearance in force, and below it are perhaps some 240
feet of shales and sandstones of the Sherburne formation.

_AXLX G*. Section along a small stream and up a steep hill about three-
fourths of a mile southeast of Sherburne village and some twenty-five feet
above the railroad. In the stream are arenaceous blocky shales in which
Hamilton fossils are abundant, especially small Chonetes.

ALIX G*. About fifty-five feet higher, near the foot of the steep hill,
are coarser shales. The fossils are not so abundant as in G', but the species
are larger, as for example, Spirifer granulosus (Con.), Hall.

AIX G*. Above comes the steep slope of the hill, completely covered
by soil to near the brow on the western side, 440 feet above G®, where occurs a
ledge composed of coarse arenaceous shales alternating with thin blue flag-
stones. Some of the thin layers contain a few fossils, as Liorhynchus mesa-
costalis, Hall; Atrypa reticularis (Lin.), Dalm.; Palwoneilo emarginata
(Con.), Hall; Paracyclas lirata (Con.), Hall; Orthis, sp.; Spirifer, sp., and
a few others. This ledge is in the lower part of the Ithaca formation and
barometrically 520 feet above the railroad, or at an approximate altitude of
1,582 feet A. T.

XTX C". One and one-half miles south of Sherburne village, Nigger

Y ¢

brook enters the Chenango river from the east. For two miles its course is

almost directly west, and it has cut a deep valley bordered by steep sides

SULTAN OT MGS WDALOM ORE

AN SA SRERRIRE,
\EZ_ON. Qopsox. \#\9_&.)

770 te =
EES =]¢ WANE On Voy Of Divide,

Covered. ANAATO.

a yowey LMAQATA Ge Weodr 04
| : \\ugger Wcllow”

. Seas =

SARRBURIV,
Wihostly Covered.

== Brow Shales Wk, GOUILOTYRES,
eS— SRLRBUAIE,

Covered.

Lee Quarry
WAQAMLETOW Sandstone Qua Shae

Wositly Covered .

A.Rievel OF Sherburne. 1042 ON

182

ProssER—HAMILTON AND CHEMUNG SERIES. 133

through the elevated tract of land which follows the eastern side of the
Chenango river for some miles. Locally, the narrow part of this valley is
known as “ Nigger Hollow.” Up this valley, one and one-quarter miles from
the river road and in a straight line about two and one-half miles southeast of
Sherburne village, is the Lee quarry which was formerly worked for a blue
sandstone at its bottom, and above this are blue argillaceous shales contain-
ing abundant Hamilton fossils. This quarry is undoubtedly in the upper
part of the Hamilton formation as may be inferred from the accompanying

list of fossils from the blue shales on top of the sandstone :

1. Spirifer mucronatus (Con.), Bill. (c)
Normal Hamilton type.

2. Spirifer Tullius, Hall. (rr)

3. Liorhynchus multicosta, Hall. (c)

Some of the small specimens show scarcely any plications on the
sides of the shell, yet they are nearer in general appearance to this

species than to Z. mesacostalis, H.

4. Orthis Vanuxemi, Hall. (1r)
5. Athyris spiiferoides (Katon), Hall. (rr)
6. Nucleospira concinna, Hall (?). (11)
7. Modiomorpha concentrica (Con.), Hall. (17)
8. Modiomorpha mytiloides (Con.), Hall. (vr
9. Modiomorpha subalata (Con.), Hall (?). (rr)
10. Palewoneilo constricta (Con.), Hall. (ir)
11. Nucula corbuliformis, Hall. (rr)
12. Chonetes mucronata, Hall (?). (zr)
13. Grammysia bisulcata (Con.), Hall. (ar)
14. Tellinopsis subemarginata (Con.), Hall. (r)
15. Lellerophon acutilira, Hall. (7)
16. Orthoceras, sp. (fragment). (11)

This quarry is barometrically 158 feet above the railroad at Sherburne.
The Hamilton shales continue at least forty-five feet higher than at the Lee
quarry, as may be seen in an outcrop of fine shales having the characteristic
lithologic appearance and fossils, by the side of the road that crosses Nigger
brook just below the forks. This outcrop is 208 feet above the railroad and
has an approximate altitude of 1,245 feet A. T., and the rocks are near the
top of the Hamilton formation as the description of those overlying will indi-
cate. The locality is one and four-tenths miles due south of the Swan quarry

which is regarded as near the top of the Hamilton formation on the northern

134 Report oF THE. STATE GEOLOGIST.

side of this hill; and if this exposure at the creek be at about the top of the
Hamilton, we would have a dip of fifty feet per mile to the south.

ATX CC®, About sixty-three feet above the Hamilton shales at the fork
of Nigger brook, on its south branch on the Ertz farm, are blackish shales.
This locality is hardly one mile above the Lee quarry, and barometrically 108
feet higher. The rocks which are well exposed along the bed and side of the
brook are even-layered argillaceous shales, part of which are decidedly blackish

in color. The shales contain a few fossils, the following species having been

obtained :
1. Glyptocardia speciosa, Hall. (1)
2. Leptodesma Pogersi, Hall. (7)
3. Coleolus aciculum, Hall (2). (c)
Slender tapering specimens without surface markings, and very
near the figures of this species.
4. Orthoceras cf. subulatum, Hall (?). (1)
5. Goniatites cf. discoideus, Hall. (c)

Very imperfectly preserved.

These shales are considered to belong in the Sherburne formation, and in
lithologic characters are quite similar to the darker shales of the Portage for-
mation in western New York.

XTX €®. Along the south branch of Nigger brook are but few outcrops
of any importance after passing the black shales of the Ertz farm. However,
at the head of the valley, two and eight-tenths miles east of the river road and
378 feet above the black shales of C?,is a ledge of thin shaly sandstones on the
G.S.Sherdin farm. These shaly sandstones form a ledge on the south side of
the highway and contain a considerable number of fossils. Spirifer mesastrialis,
Hall, is common, several specimens preserving the external surface of the shell
and showing clearly the markings of the fine striae which characterize this
species. Two specimens are very broad, like that shown in figure 18, plate XL,
Vol. IV of the Paleontology of New York, and there can be no doubt as to
the correctness of the identification of this species. Professor Clarke has
suggested that the appearance of the above species is evidence of a change
from the Hamilton to the Ithaca formation.’ JI would also state that this
species is generally above the first species of this fauna, and is not present
until the Ithaca fauna is fairly well represented. A search of twenty minutes

in these thin sandstones furnished the following :

1 Thirteenth Annual Report State Geologist [New York], p. 554.

Bs

2.

ili

12.
138.
14.
15.
16.

ProssER—HaAMILTON AND CHEMUNG SERIES. 135

Spiriter mesastrialis, Hall. (c)
Several specimens of the exterior clearly show the striae, so there
‘an be no doubt as to the species.
Spirifer mucronatus, Hall. (c)
These specimens are small and mucronate with few plications.
In the interior of one is a small septum showing the beginning
of that character. These are like many of the Ithaca speci-
mens, and probably it would be better to call them varieties of
this species.
Spiriter granulosus (Con.), Hall and Clarke. (rr)

Two external impressions which have distinct pits that must
have been made by pustules, and the impression of the dorsal

valve shows a small furrow along the center of the fold.

Cyrtina Hamiltonensis, H. (2). (rr)
Broken and poorly preserved specimen.
Chonetes scitula, H. (a)
Chonetes setigera, Hall. (c)
Smaller specimens with fewer and coarser striae having form of
this species and spines at the same angle from the hinge line.
LTehynchonella (Camarotachia) Stevens’, Hall. (ce)

Two or three specimens approach the 2. (C.) eximia type.
i Pp} j

Tropidoleptus carinatus (Con.), Hall. (1)
Atrypa reticularis (Lin.), Dalm. (r)
Stropheodonta perplana (Con.), Hall (2). (rr)

Poorly preserved.
Orthis, sp. (1r)
Not poorly preserved but apparently nearer in form to
O. Vanuxemi, H., than to O. ¢mpressa, H.

Palwoneilo emarginata (Con.), Hall. (rr)
Modiomorpha mytiloides (Con.), Hall. (ar)
Modiomorpha concentrica (Con.), Hall. (rr)
Paracyclas lirata (Con.), Hall. (rr)
Palwoneilo constricta (Con.), Hall. (ar)

From the above fauna this ledge is referred to the Ithaca formation, but

it is probably fully 100 feet above its base. The approximate altitude of the
ledge is 1,686 feet A. T., and the altitude of the lowest Ithaca fossils on the top
of the hill above the Swan quarry is 1,544 feet. This locality is two miles

136 REporT of THE STATE GEOLOGIST.

southeast of Swan hill, so that, making an allowance for dip, it is probable
that C® is nearer 150 than 100 feet above the base of the Ithaca formation.
AXIX (€* One mile farther east, in the southwestern corner of Colum-
bus, rocks are seen by the side of the road. This place is on top of the divide
between the Chenango and Unadilla rivers, from which a beautiful view of
the surrounding country may be obtained. These rocks are the highest of
this region, by the barometer 126 feet higher than C*, 567 feet above the
Hamilton at the Nigger brook crossing, and 770 feet above the railroad in
Sherburne village, giving an approximate altitude of 1,812 feet A. T. They
consist of micaceous and arenaceous shales and shaly sandstones, part of the
layers containing plenty of fossils, and others scarcely any except an occasional
lamellibranch. The following species were collected in fifteen minutes :
1. Spiriter mucronatus (Con.), Bill. var. posterus, Hall and Clarke. (aa)
These specimens in general seem to be like figures 28 and 30,
(plate XX, Palaeontology of New York, Vol. VILL, Brachio-
poda IT.) of this variety, although some might possibly be referred
to the species itself. The internal impressions in the umbonal
region of two or three specimens show a small groove which looks
as though they might have possessed a small septum and these
should be compared with Sp. mesacostalis, although I have seen
Sp. mucronatus with a septum in the Hamilton (Moscow) shales
of Cayuga lake.
2. Spirifer granulosus (Con.), Hall (2). ar)
Part of an external impression that shows very clearly the im-

pressions of pustules.

3. Liorhynchus mesacostalis, Hall. ar)
4. Paracyclas lirata (Con.), Hall. ar)
5. Nueula corbuliformis, Hall. ar)
6. Palwoneilo cf. filosa (Con.), Hall. (7)

Impressions that do not preserve any of the surface markings
except near the outline of the species.

7. Modiomorpha ct. subalata (Con. ), Hall, var. Chemungensis, Hall. (r)

5. Leptodesma Roger si, Hall (2). (7)
9. ctinopteria perstrialis, Hall. (ir)
10. Schizodus ef. AppVressus (Con.), Hall. (rr

The upper 800 feet of this ridge, which includes the highest

rocks of the divide, belong in the Ithaca formation.

ProssErR-——Haminron AND CHEMUNG SERIES. 137

; North Norwich.

XI A’. The next township south of Sherburne is North Norwich, in
the northwestern portion of which is a steep and high hill, known locally as
Pratt’s mountain. On its eastern side is the Chenango river, and on the
western the Fly brook valley, which is followed by the Delaware, Lackawanna
and Western railroad from the North Norwich station to Sherburne village.
On the eastern side of the hill, two and four-tenths miles south of Sherburne,
and immediately above the lock on the abandoned Chenango valley canal, are
rather coarse, arenaceous shales in which Hamilton fossils are common. This
exposure is about on a level with the station in Sherburne.

AL A*. This part of the hill side is very steep, and near its top,
345 feet above the canal, is a ledge composed of thin arenaceous shales
alternating with thin sandstones, an inch or more in thickness. Fossils are
very rare, only a few specimens of Liorhynchus bemg found. The outcrop is
probably in the Sherburne formation, although not far from the base of the
Ithaca, and it has an approximate altitude of 1,387 feet A. 'T.

XL 7, The southern end of Pratt’s mountain is about one-half mile
north of the village of North Norwich, and near the brow of the hill are
coarse, arenaceous shales that split into thin, somewhat even pieces. Fossils
are.very rare, an occasional Liorhynchus and Spirifer with fragments of plant

stems constituting all that were found. This is probably the base of the

oO
Do
Ithaca formation. The New York, Ontario and Western railroad station at
North Norwich is 1,005 feet A. T., but probable inaccuracy in the readings of
the barometer on account of rain gave this ledge as 265 feet higher than the
station, which would indicate an altitude of 1,270 feet A. T.

OI OLS Along Cold brook, about one mile southwest of North Norwich,
are bluish arenaceous shales that split into regular pieces of uniform thick-
ness. No fossils were found except fragments of plant stems. The first
exposure of these shales was at eighty-five feet above the station, and they
continue with practically the same characters for 153 feet and belong in the
Sherburne formation.

EGE GO*: Along a small stream that enters Cold brook from the west are
rocky cliffs, and at an elevation of 1538 feet above the railroad, or approxi.
mately 1,158 feet A. T., is a layer, about two inches thick, containing fossils,
mostly brachiopods, as Léorhynchus mesacostalis, Hall; Spirifer mesastrialis,
Hall (7): Spiriter mucronatus (Con.), Bill. (Ithaca variety); Cyrtina Hamiat-
tonensis, Hall; Nuenla sp. and Crinoid stems. This exposure is clearly the

first of the Ithaca fauna, and may be considered the base of the Ithaca forma-

MDD BAI SESTOK, SHUT
WEST DE VLORTA TORU,
(Fay. .\

300 QT. Apysos.

ch Sandclone UCHACA.

195°
Covered.
07 = , Wilkes Quassy, Sandslones Onda
fe: ~ =|" _. Shales
Eossuls Common

Wyostly, Covered.

Base O¢ VTAKCQH.
SPLATTER MESOS TRL

SUERBARAG.
ver ee ee

Covered |

RR. egvel Od ost K\oswrely.
ood QM

ProsserR—HAmIttTon AND CHEMUNG SERIES. 139

tion which, on top of the high hill southwest of Smyrna village, is seven miles
northwest of this locality. The approximate altitude of the Smyrna locality
above sea level is 1,620 feet, and that at North Norwich is 1,158 feet, making
a dip of sixty-six feet per mile to the southeast between these two localities,
which is greater than had been given in previous estimates.

XL ©. About one and one-half miles southwest of North Norwich, in
the edge of Plymouth township, is the Horace Wilkes quarry which, fifty
years ago, was worked under the name of the Harris quarry. It is about 412
feet above the railroad, or 1,417 feet A. T. The back of the quarry shows
about twenty-five feet of blue sandstones alternating with shales. A small
amount of the stone is quarried for flagging, but most of it for building pur-
poses. The sandstone contains specimens of Spérophyton velum, Van., of large

size, and other fossils are common. The list is as follows:

1. Spirifer mucronatus (Con.), Bill. (c)
2. Atrypa reticularis (Linné), Dalm. (ce)
3. Liorhynchus mesacostalis, Hall. (c)
4. Chonetes scitula, Hall (2). (a)

This species is abundant, but in the condition of impressions
which renders identification difficult. Some of the specimens
approach C. setigera, Hall, in form, though they are not so convex

near the umbo as those found at Ithaca.

5. Chonetes lepida, Hall. (ar)
6. Cyrtina Hamiltonensis, Hall. (ir)
7. Stropheodonta sp. (rr)
Two imperfect impressions which are similar to S. perplana
(Con.), Hall.
8. Productella, sp: (c)
9. Microdon (Cypricardella) bellistriatus (Con.),
Hall, or VW. tenuistriatus, Hall. (11)
A single specimen that has the proportions of JZ. be//istriatus,
as well as those of the elongated form of JW. tenudstriatus, Hall
(see plate 73, figure 28, Palaeontology of N. Y., Vol. V., Part I).
It is impossible to determine whether the specimen has the fine
striae of JZ. tenwistriatus or the coarse striae of VW. bellistriatus.
10. Paracyclas lirata, (Con.), Hall. (ir)
11. Cimitaria recurva (Con.), Hall. (1)
12. Palewoneilo emarginata (Con.), Hall. (rr)

13. Goniophora carinata (Con.), Hall (2). (1)

140 Report oF THE STATE GEOLOGIST.

This species is reported from Copley’s quarry at Oneonta.’ A
comparison of specimens from the two localities fails to prove them
precisely similar; but the North Norwich specimens are nearer

this species than any of the others figured in this work.

14. Modiomorpha, sp. (a broken specimen). (ar)
15. Glossites depressus, Hall. (1r)
A single specimen that apparently belongs to this genus and
species.
16. Palwoneilo constricta (Con.), Hall. (1r)
7. Orthis, sp. (rr)
18. Leptodesma cf. Rogersi, Hall. (1)

These specimens do not have as mucronate ears as most of those
figured ; but some of them resemble closely the one figured on
plate 21, figure 9 (Palaeontology of New York, Vol. V., Part L.,
Lamell. I.), which is stated to be from the Hamilton shales at
Norwich, N. Y.

19. Orthothetes Chemungensis (Con.), Hall. (r)
20. Actinopterta Boydi (Con.), Hall. (rr)
21. Phacops rana (Green), Hall. (rr)

22. Sptrophyton, sp.

The « juarry is of course in the Ithaca formation, and some 260 feet above
its base. Vanuxem mentioned the quarry, referring the rocks to the Ithaca
group and called it the second best locality for the “Hucoides velum, or Curtain
Fucoid” — Spirophyton, and stated that “fossils are somewhat numerous.” *

AL (C*. On top of the hill, above the Wilkes quarry to the west of
Cold brook, is an outcrop of sandstone in the South Plymouth road, which 1s,
perhaps, 495 feet above the North Norwich railroad*station, making its alti-
tude approximately 1,500 feet A. T. The sandstone weathers to a brownish
color, contains large numbers of Spirifers, and is in the Ithaca formation, which
gives a thickness of 340 feet to this formation in the hill southwest of North
Norwich.

Norwich.

XXXV C*. South of North Norwich is Norwich township which has
been carefully described by J. M. Clarke,’ and those interested in the geology

of the Chenango valley are referred to that report for the description of this
1 Palaeontology of New York, Vol. V., Part I., Lamell. II., p. 302; see plate 44, figure 7, for figure of form similar to the North
Norwich specimen.
2 Geology of New York, Part III., 1842, pp. 178, 293.
3 Thirteenth Annual Report State Geologist [New York], pp. 533-539.

Pross—ER—HamiItron AND CHEMUNG SERIES. 141

township as well as those of Oxford and Greene to the south. A few localities
were studied by the writer that are not mentioned by Clarke, and a_ brief
description of them may add something to our knowledge of the geology of
the township.

About one-quarter of a mile north of the Delaware, Lackawanna and
Western railroad station in Norwich village, is a railroad cut through bluish
shales and shaly sandstones. The base of the cut is not more than ten or
fifteen feet higher than the railroad station, which is given.as 1,001 feet A. TY
Fully five feet of rocks in which fossils are common, are exposed in the cut,
g large numbers of Liorhynchus mesacostalis,
Hall; Chonetes setigera, Hall, and Spirifer mucronatus (Con.), Bill. The

following species were collected :

some of the layers containin

1. Liorhynchus mesacostalis, Hall. (aa)
2. Chonetes scitula, Hall. (a)
3. Chonetes setigera, Hall. (aa)

This narrower species with the smaller number of striae is by far
the most abundant specimen from the railroad cut. Some of the
specimens show a tendency towards C. /epida, Hall, in the character
of two stronger striae near the center of the shell and finer ones
between them.

4. Spirifer mucronatus (Con:), Bill. (aa)

These specimens agree fairly well with figures of this species, as
figures 1, 4,19, and 20 of plate 34 (Palaeontology of New York, Vol.
IV.), and are undoubtedly the same as the forms listed by Clarke
from Norwich as this species (Thirteenth Annual Report, p. 533,
etc.); but there are specimens from Ithaca that are difficult to
separate from some of these. There are both mucronate and
rounded forms.

5. Spirifer granulosus (Con.), H. and C, (?). (r)
One impression which shows very clearly the numerous pittings

produced by the pustules.

6. Atrypa reticularis (Linné), Dalm. (rr)
7. Tropidoleptus carinatus (Con.), Hall. (c)
8. Productella, sp. (c)

Poorly preserved and broken specimens, possibly nearer

P. dumosa, H., than P. speciosa, H.

1 The profile of the New York, Ontario and Western railroad gives the Norwich station as 987 feet A. T., and it seems hardly
possible that there is a difference of fourteen feet between the two railroad stations in the village.

142 Report OF THE STATE GEOLOGIST.

9. Stropheodonta, sp. (1)
I have compared these with S. mucronata, (Con.), H., and

S. perplana (Con.), H., without coming to a decision as to their
specific character. They seem to be rather too convex for the
former and too much variation in the size of the striae for the latter.

10. Palwoneilo fecunda, Hall. (rr)

The specimen seems to be nearer to this species than to P. filosa
(Con.), Hall. The geatest length is not on the hinge line.

11. Cyrtina Hamiltonensis, Hall. (rr)

This locality is, of course, in the Ithaca formation and some distance
above its base.

XXX V At. Clarke described an interesting section on the western
side of Canasawacta creek along the road northwest from Norwich toward
Preston,’ and the writer studied one beginning on the Canasawacta creek in
the western part of the village, and following the road up the steep hill
directly west. This hill affords a section of 550 feet, and on account of its
close agreement with the one described by Clarke, it is considered suffi-
ciently interesting to merit a description. On the bank of Canasawacta creek,
immediately below the bridge at the western side of the village, are thin,
irregular sandstones and coarse, arenaceous shales. Some clay pebbles are
found in the rocks. Fossils are common in some of the layers, as Tropidolep-
tus carinatus (Con.), Hall; Chonetes scitula, Hall; Spirifer mesastrialis,
Hall (7) ; Fhynchonella sp., and lamellibranchs. This outcrop is sixteen feet
below the highway bridge, or approximately 985 feet A. T., and is in the
Ithaca formation, though somewhat above its base. The base of the Ithaca
formation on the branch of Cold brook, one mile southwest of North Norwich
is five and four-tenths miles north of the above locality, with an altitude of
1,158 feet A. T., which indicates that the dip between these two places is
greater than thirty-two feet to the mile; how much greater is not known, as
the base of the Ithaca formation has not been noted in the vicinity of Norwich.

XXX V A® This is an old quarry a little beyond the forks in the road
and 155 feet above the creek level, in which forty feet of rocks are exposed,
consisting of blue sandstones alternating with shales, some of the layers con-
taining clay pebbles. The sandstones are of irregular thickness, some of them
about two feet thick but generally much thinner. Fossils in general are not
numerous though some layers are composed largely of a few species forming

what might be called a firestone. The most abundant fossils are: Paracyclas

1 Thirteenth Annual Report State Geologist [New York], pp. 534-539, with section on p, 538.

ProssER—HaAmILTON AND CremuNnG SrErIEs. 143

Virata (Con.), Hall; Chonetes scitula, Wall; Atrypa reticularis (Lin.), Dalin.;
Palewoneilo maxima (Con.), Hall; and Spirifer, sp. The top of this quarry is
208 feet above the creek level, which brings it in an approximate horizon
with stations B and B,, described by Clarke,’ who gave a list of nineteen
species. For about eighteen feet the rocks are covered and then arenaceous
and rather smooth shales that weather to a greenish tint are exposed by the
roadside, The base of these shales is 226 feet above the creek and they show
a thickness of nineteen feet on the road. At 239 feet above the creek in thin
blocky shales a few fossils were found, Paracyclas lirata (Con.), Hall, and
Microdon (Cypricardella) bellistriatus (Con.), Hall. In a thin sandstone layer
are plenty of crinoid segments. These were the last fossils noted until the
red and grey rocks were reached above at an elevation of 491 feet.

XXXV A?® is used to designate the shales and rather coarse sandstones
after fossils become very rare. At 277 feet above the creek are very fine,
smooth and micaceous shales that break up into small pieces about an inch
square. At 386 feet rather coarse-grained sandstones begin to appear.

XXXV A‘. These coarse sandstones with a little shale continue to an
elevation of 426 feet where a stratum of coneretionary coarse-grained sand-
stone weathering to a greenish tint, crosses the road, below which are thin
shales without fossils. Fifty feet higher a prominent, coarse-grained grey
sandstone crosses the road.

XXXV A*®. At 491 feet above the creek level is the first outcrop of
red argillaceous shale, below which is fissile, argillaceous, olive shale. About
three feet above the base of the red shale is a slightly calcareous layer that
contains clay pebbles with flat, black fish scales and fragments of fish bones.
The red shales were not noticed on the road section above 517 feet. It is
interesting to note that Clarke described an outcrop of “about three feet of
soft red and green sandy shales with minute fish bones and entomostraca” on
the Norwich-Preston road about one mile northwest of this locality.” The
altitude of this red shale above the river level is, according to Clarke, 495 feet.
This agrees very closely with that of the fossiliferous red shale described by
the writer at an altitude of 491 feet above the level of Canasawacta creek,
which can differ but slightly from the river level at this locality.

XXXV A®. Near the brow of the hill is the Crandall quarry, no longer
worked, the top of which is 551 feet above the creek level, or approximately

1,536 feet A. T. The rock is a coarse-grained, greenish-grey sandstone, whose
b] fo) (2 ro) .

1 Thirteenth Annual Report State Geologist [New York], pp. 534 and 535,
2 Thid., p. 536.

SECTAOY, WEST OE
VORA
a5. OQ.

B52 AT Qpyros.

[' o& opr 04 Crondeall Quarry.

BOWTOA
SS > Red Shales. aceles OF

OG CoO 6

A276 (cereserese
SSSSSSS==SS=SS—Sa
S¥RGray Sen geearees

CaP IOS J} Ce ac

is
OX we son “Coarse Gray Sandstone.

a UTRQCO.,

Coasse Groaned Somastones

Rarity, Covered.

O
Smooth, K\reaceous Shales

CVoveyea
Green s\ Shales MM O Few

Bossuks
Covered

Brue Shales And Soandstones
OF Dla Quasry

Covered

Shales Qna Sandstones
AN RACH.

Laewel Cangsawacla Creek.
905'OA.°,

144

Coarse Greenish Gray Sandsione

Red Shale hee 0% OHEDNTA,

LORACYCUOS ARAN O

ProssER—HaAMILTON AND CHEMUNG SERIES. 145

layers are separated by shales. One layer in the upper part of the quarry is
two feet thick, and another near the bottom is a finer-grained stone twenty-
seven inches in thickness. Similar greenish-grey sandstones continue to the
top of the hill some fifteen feet higher, 567 feet above the creek level or
approximately 1,557 feet A. T. Below the base of the red shales, 491 feet
above the creek, in the above section, fossils are very rare for a thickness of
252 feet, in that portion of the section that is indicated as A‘ and A®, Pro-
fessor Clarke observed that in the Crandall quarry, the base of which is 465
feet above the river, “fossils are exceedingly and remarkably rare through-
out,” but he was fortunate in finding a few in one of the flagstones, and they
are here listed: “ Palwoneilo emarginata, small form; Nuculites lirata, small
form, and Leda diversa. After a long search the soft green shales produced

Ce shies outcrop is less

a single specimen of a small Orthoceras or Coleolus.
than twenty-five feet below the fossiliferous red shale. These sections show
very clearly the gradual transition from the fossiliferous blue shales and
sandstones of the Ithaca formation to the coarser greenish-grey sandstones and
argillaceous red and green shales of the Oneonta formation, the conditions of
which were unfavorable to marine life. Farther east these conditions began at
an earlier period so that it is almost impossible to draw a synchronous line of
separation between the Ithaca and Oneonta formations when followed from
the Chenango valley eastward into Schoharie and Albany counties.

The first heavy greenish-grey sandstones have been considered the base
of the Oneonta formation by some geologists, while others have placed the
lowest red shales there. It seems probable that in either case the line will be
a somewhat variable one. Apparently Clarke considered the base of this
formation defined by the “light grey-green sandstone” of the Hale quarry,’
northwest of Norwich, which is 510 feet above the river level. Possibly it
might be as well to regard the red shales with the fossil fish remains eighteen
feet lower as the base, although, as previously stated, the line will vary in
position when followed for some distance. If these red shales are called the
base of the Oneonta formation, then in the high hill west of Norwich and the
Canasawacta creek, the Ithaca formation has a thickness of 490 feet, show-
ing its entire thickness to be greater than 500 feet for the Chenango valley.
It is to be recalled that a thickness of 450 feet has been assigned to the rocks

of the latter formation in the vicinity of Ithaca.’

1 Thirteenth Annual Report State Geologist {New York], p. 536,

2 Thid., p. 536, 587. Darton states that in Albany county he assumed the base of the Oneonta formation to be *‘ at the bottom
of the lowest red shale member;”’ ébid., p. 240.

3 Transactions American Institute of Mining Engineers, Vol. XVI., p. 945.

10

146 Report oF THE STaTE GEOLOGIST.

AXYXV £B. Quarry three miles northwest of Norwich, in the south-
eastern corner of Plymouth, and on the western side of the Canasawacta creek
above the former DeRuyter branch of the New York, Ontario and Western
railroad. This quarry is in the Ithaca formation and is between ninety and
one hundred feet higher than the Norwich railroad station. About twenty
feet of blue sandstone and shales are exposed. Fossils are common in the
lower layers, but few were seen in the upper part of the quarry. Z/opi-
doleptus carinatus (Con.), Hall; Spirifer mucronatus (Con.), Bill.; Lio-
rhynchus mesacostalis, Hall; Productella, sp.; Palwoneilo, sp., and some
other species are common. A church in Norwich was built of stone from this
quarry.

XXXV LD. The lowest rocks in Ransford creek, about one and one-
quarter miles northeast of Norwich and some forty feet above the railroad
station, consist of thin blue sandstones and shales. Ziorhynchus mesacostalis,
Hall, and Spirifer mucronatus (Con.), Bill, are abundant. A little farther
up the creek is a quarry in blue sandstone alternating with shales. There is
no flagging, and the stone is used for building purposes only. Fossils are
quite common, Zropidoleptus carinatus (Con.), Hall, and Productella, sp., are
most abundant. One good specimen of Cimitaria recurva (Con.), Hall,
was found,

XXXV LP, On Ransford creek, two miles northeast of Norwich, is the
reservoir, the top of the dam being 160 feet above the railroad station, or
1,160 feet A. T. In the creek, Just below the dam, are shales and sandstones
which in places contain abundant fossils, especially Liorhynchus mesacostalis,
Hall; Paracyclas lirata (Con.), Hall; Spirifer, sp., and Rhynchonella, sp.
Above this locality, at about the same level as the dam, is a quarry that was
opened when the reservoir was built. The rocks are blue shales and sand-
stones in which fossils are common, Chonetes and Spirifer being the most
numerous. These exposures described along Ransford creek are in the

strongly fossiliferous portion of the Ithaca formation.

All the recent writers in describing the geology of the Norwich region
have noted the great similarity between the fauna of the Ithaca, as exposed
in the Chenango valley, and that of the Hamilton formation. Professor H. 8.
Williams, in 1886, stated that “the fauna A‘ | which he called the Paracyclas
Jirata stage of the Hamilton faunas occurring above the horizon of the
Genesee shale|, underlying the greys which initiate and terminate the reds

[the Oneonta formation | was composed of Hamilton species with scarcely any

ProssER—HamiILtTon AND CHEMUNG SERIES. 147

exception—that is, species that are known to occur below the second black
Devonian shale.”

The writer referred to this fact in 1893, and Clarke, in 1894, stated it
very clearly. In describing the faunas near Norwich, Clarke wrote: “If,
however, there exists a palpable difference between the faunas at B and B,
[quarries one mile northwest of Norwich], and that of the typical upper
Hamilton shales in regions where the Tully limestone is present, they may be
reduced to the existence in the former of Actinopteria zeta, and the not

73

infrequent occurrence of Spirifer mesastrialis;”* and again “the predom-

inant traits of the fauna are Hamilton; its extra-Hamilton species are rare,
especially in the lower parts of the series.” *

As will be seen from the above statement, the rocks near Norwich con-
tain a considerable number of species that occur in the Hamilton formation,
but have not yet been reported from the Ithaca formation as exposed at its
typical locality, Ithaca. Since this fauna is more decidedly Hamilton than
the typical Ithaca, which is the general condition at least from the Chenango
valley eastward, the question may arise whether eventually it may not be
better to designate this formation by a name that will refer to a locality at
which the faunal and stratigraphic conditions are more nearly representative
for the eastern and greater extent of the formation.

While considering this portion of the Chenango valley section it is
important to remember that in most of the recent papers relating to the
geology of this valley, the Sherburne formation has been overlooked. As
described above in Nigger brook, in the southern part of Sherburne township
(XIX C*), in the lower part of the Sherburne formation is a Goniatites fauna
that is probably an eastern extension of the Cephalopod stage (C') described
by Dr. H. 8. Williams as occurring in the lower Portage.® The writer called
attention to this formation in 1887,° although at that time, on account of in-
sufficient data, its thickness was underestimated, and again in 1893." The
Sherburne formation in the Chenango valley is 250 feet in thickness and the
Ithaca formation at least 500 feet, making a total thickness, for the rocks,
from the top of the Hamilton formation to the base of the Oneonta, of more
than 750 feet. This gives a thickness of some 1,250 feet for the Sherburne,

1 Proceedings American Association for the Advancement of Science, Vol. XXXIV., p. 229; also see the plate of ** Meridional
sections of the Upper Devonian deposits of New York, Pennsylvania and Ohio,’’ section TX.

2 American Journal of Science, Third series, Vol. XLVI., p. 225.

3 Thirteenth Annual Report State Geologist [New York], p. 535.

4 Tbid., p. 554.

5 Proceedings American Association Advancement of Science, Vol. XXXVL., p. 226.

6 Ibid., p. 210.

7 American Journal of Science, Third Series, Vol. XLVI., pp. 221, 222, 224.

148 Report oF THE STATE GEOLOGIST.

Ithaca and Oneonta formations of the Chenango valley, which is only fifty
feet less than the thickness of the lower Portage, Ithaca and upper Portage
in the vicinity of Ithaca, consequently the position of the Oneonta formation
is nearly in line with the upper Portage of the Ithaca section, and the
Portage sandstones of the Naples and Genesee sections. Clarke has advanced
this correlation and stated “that these Oneonta beds (including the barren
grey sands and flags lying beneath the red and green shales and sands) are
the eastern representative of the upper sandstones and flags originally desig-
nated by Professor Hall as the ‘ Portage sandstones,’ and are hence the sedi-
mentary equivalent of the typical Portage.”

Oxford.

Along the Chenango river valley to the southwest of Norwich is Oxford
township. Except along the immediate valley of the Chenango river in the
northern part of the township where the Ithaca formation occurs and in the
southeastern part where the Chemung is found, the township is covered by
rocks of the Oneonta formation, and its geology was so fully described by
Professor Clarke in the Thirteenth Annual Report, that little remains to
be said.

XLII A’. The farthest south that the Ithaca formation was noticed, is
a characteristic outcrop of shales containing plenty of fossils along the side
of Fly Meadow creek, near the highway one and one-half miles northeast of
Oxford village.

XLII ££". Nearly three miles northeast of Oxford village in the north-
eastern corner of the township is Lyon brook, across which is the noted
Lyon brook bridge of the New York, Ontario and Western railroad. The
bridge is 161 feet above the bed of the stream, and has an altitude of 1,197
feet A. T. In the bed of the brook beneath the bridge, as well as north of
the highway to the east of the bridge, are bluish shales, in which a few
rather poorly preserved fossils occur. Small lamellibranchs are the most
common, This locality was studied by Dr. C. E. Beecher, Dr. J. W. Hall,
and Mr. C, E. Hall, who reported “ Spirifer mesastrialis, Paracyclas lirata,
and Palwoneilo muta” from these shales, which were stated to be “ below the
red shales which occur about two hundred feet higher in the series.”* This
outcrop is in the upper part of the fossiliferous portion of the Ithaca forma.

tion. On the south side of the brook and about sixty feet higher, a quarry

1 Thirteentb Annual Report State Geologist [New York], p. 557. See also similar statement near the middle of p. 555 and the
section on p. 556
2 Fifth Annual Report State Geologist [New York], 1886. p. 11; see page 4 for credit.

ProssER——HamIuron AND CHEMUNG SERIES. 149

in bluish-grey to buff sandstones was opened by Mr. Burns, but the stone did
not prove valuable.

XLI B*. Still higher than the Burns quarry is one that was opened
‘during the construction of the railroad and furnished stone for the abutments
of the bridge. At the bottom of the railroad quarry are grey sandstones,
then red sandstones that are capped by red shale. The red rocks are about
thirty feet below the railroad track, or 1,167 feet A. T. If these reds corre-
spond to the lowest reds in the hill west of Norwich, and they seem to have
that position, then they will give the dip along almost a direct north and
south line. The red shales west of Norwich are 1,476 feet A. 'T., and the
distance between the two places four and eight-tenths miles, giving us a dip
to the south of 64* feet per mile.

To the south of the bridge there are railroad cuts through coarse-grained,
greenish-grey sandstones, alternating with red shales, which show clearly
enough that these rocks are in the Oneonta formation. In these shales
specimens of a fern—Archwopteris sp—were found. Farther south, near the
middle of a cut through the coarse grey sandstone, just north of the 218th
New York mile post, are numerous fragments of plants, among which is
Lepidodendron Gaspianum, Dn. In the same cut, specimens of the character.
istic fossil of the Oneonta sandstone, Amnigenia Catshillensis (Van.), Hall,
oceur, and an unusually good specimen of Holonema rugosa (Claypole), Newb.,
was found. This specimen of a fossil fish has been described by Professors
H. 8. Williams,’ Claypole? and Cope,? while the last edition of Dana’s Manual
of Geology contains a figure showing the restored ventral plates of the
species. In addition to the above species, Leptodesma Rogersi, Hall, was
reported, probably from this cut.

ALL (. A railroad cut on the New York, Ontario and Western railroad,
about two and one-half miles southeast of the Oxford station and one-quarter
of a mile north of the 214th New York mile post. The cut is through red
and greenish shales, alternating with thin grey sandstones. The dip is at least
sixty feet to the mile, twenty degrees west of south. A layer of the nature
of a conglomerate, containing an occasional quartz pebble, was noticed.
Fucoidal markings occur in the grey sandstones, while in thin layers quite
a number of fossil shells are preserved. The following species from this cut
are listed in the Fifth Annual Report of the New York State Geologist :

1 Proceedings American Association Advancement of Science, Vol. XXXIX., p. 337.
? American Geologist, Vol. VI., pp. 255-257.

3 Proceedings United States National Museum, Vol. XIV., p. 456.

* Fourth edition, 1895, fig. 953 on p. 616; see also p. 618.

5Fifth Annual Report State Geologist [New York], p. 11, 2d paragraph.

150 Report oF THE STATE GEOLOGIST.

“ Macrodon Hamiltonie, Actinopteria Boydi (2), Actinopteria sp. (2), Modio-
morpha subalata (2), Leptodesma sp., Strophodonta perplana.”'! The altitude
of this cut, taken from the profile of the New York, Ontario and Western

railroad, is approximately 1,560 feet A. T. This locality is three and one-half.

miles west of south of Lyon brook bridge, and the difference in altitude
between the base of the red shale and this cut is 348 feet. If the dip for
the distance is sixty feet per mile, then the thickness of the rocks is 558 feet,
all of which may be regarded as belonging in the Oneonta formation.

XLII C?. One-fourth mile southeast of Summit station, or five miles
from Oxford station, is another railroad cut, through greenish and olive shales
and sandstones, which reveals a thick concretionary stratum. Fossils are not
uncommon in these rocks, the most abundant species being Atrypa reticularis
(Lin.), Dal. while “ Productella hirsuta, Spirifer mesacostalis, and other
species ” have been reported.” From the railroad profile the altitude is 1,616
feet A. 'T., or fifty-six feet higher than the cut at C', which is probably near
the top of the Oneonta formation, for at C? no red or coarse greenish-grey
rocks were seen, and the Summit beds have been referred to the “ Lower
Chemung group.”?

The extensive stone quarries of the F. G. Clark Company, at Oxford, in
which specimens of Amnigenia Catskillensis have been found, and the Miller
quarry at South Oxford are both in the Oneonta formation, and were fully
described by Clarke in the Thirteenth Annual Report, to which the reader
is referred for an account of the excellent flagging stones of this formation.‘
The picture of the Clark quarry shows the massive character of this

sandstone.
Greene.

To the southwest of Oxford is the township of Greene, which is crossea
diagonally from the northeast to the southwest by the Chenango river. The
Oneonta formation follows the river valley as far south as the village of
Greene, but the remaining and greater portion of the township is covered by
rocks which, on the new Geological Map of: New York, are placed in the
Chemung formation. The northern half of this township was fully described
by Clarke,’ who referred the greenish fossiliferous shales and sandstones

overlying the Oneonta formation to the Chemung. Southeast of Greene

1 Loc. cit., p. 11, 3d paragraph.

+ Ibid., p. 11, 4th paragraph.

3 Ibid., and compare the section at the bottom of the page

4 Tbid., pp. 589-542.

5 Thirteenth Annual Report State Geologist [New York], pp. 542-546.

ProssER—HAMILTON AND CHEMUNG SERIES. 151

village is Juliand hill, whose summit is some 300 feet above the river level,
and whose upper half is mainly composed of greenish argillaceous shales.
Clarke, in describing this hill, stated that “fossils are abundant throughout
these shales, and are of typical Chemung expression, viz:

Atrypa reticularis, large, rugose ; common.

Orthis impressa, large form; abundant.

Liorhynchus globuliformis, common.

Spirifer: mesacostalis.

Productella lachrymosa,

Stropheodonta perplana var. nervosa.

Cryptonella, sp."

In the lower part of the greenish or Chemung rocks, near the north-
western corner of the corporation of Greene village, is a sandstone containing

coarse quartz pebbles which, some years ago, the writer designated as the

Greene conglomerate. This stratum contains fragments of fossil fish, as stated
by Clarke, who writes that the lower part “contains Ho/onema ct. rugosa,

Claypole, undetermined plates, scales and teeth.”’

In the same exposure, but
a little higher, Clarke noted “fish remains common,” and “ Lingula cf. Cuya-
hoga, Leptodesma ct. sociale (single specimen)”.? To the southwest of the
village is the old Cameron quarry. The lowest rocks of this quarry contain
scarcely any fossils except Zéentaculites sp. and large Crinoid segments, while
the shaly layers of the upper part of the exposure contain fossils, but of only
a few species. This quarry was described by Vanuxem, who stated that it
was the “only opening noticed in the hills at Greene,” and referred it to the
Chemung group.’

XXXVI A'. In the extreme southwestern corner of Greene township
are the villages of Williards and Chenango Forks. On the hillside west of the
Utica division of the Delaware, Lackawanna and Western railroad, between
Chenango Forks and Williards, is an old quarry that was opened during the
construction of the Chenango canal and is not worked at present, the base of
which is about sixty-three feet above the railroad track. The rocks consist
of blue, argillaceous, thin or shaly sandstones, separated by blue shales, all of
which weather to an olive tint.

Fossils are common in most of the rock and abundant in layers. Pro-

ductella lachrymosa (Con.), Hall; Spirifer mucronatus (Con.), Bill, var.

1 Thirteenth Annual Report State Geologist [New York], p. 543.
2 Tbid., p. 545.

3 Thad.

+ Geology of New York, Part ITI., 1842, p. 293.

152 Report oF THE STATE GEOLOGIST.

SECTION BENUREL WTLAAIS
OND CALMONGS CORKS.

(#36. 0.)
wes AN. Oypros,
265.

O CHAEMUNG. Leosse Brooks Wen
WORAUMCAUS GQUOBUWLAL-
CORMUS Onda LARLOPE CTE

TRATOSTOVLUS

CHEMUNG,
Q Ora Quarry lu Which Ave

6 3' OQoundont Bossils.

R. Rive Or Chenango Yorks. 90/ ON.

posterus, Hall and Clarke; Orthis impressa, Hall, and Crinoid segments are
the most abundant species. The complete list is:
1. Orthis impressa, Hall. (aa)
Large form as reported by Clarke from southeast of Greene
(Thirteenth Annual Report, p. 543).
2. Productella lachrymosa (Con.), Hall. (aa)
Probably some of these specimens should be ef. P. speciosa of
Ithaca, but the pustules are coarser than in this species. So
identified by Clarke in Thirteenth Annual Report, p. 543.
3. Spirifer mucronatus (Con.), Bill., var. posterus, Hall and Clarke. (aa)
Many of these specimens agree exactly with the figures of the
mucronate forms of this species. These are undoubtedly the
same as those from Chenango identified as Sp. mucronatus var. by
Professor H. 8. Williams and figured in Bulletin Geological
Society of America Vol. L, pl. 12, £..13.

ProssER-—HAMILTON AND CHEMUNG SERIES. 15:

Ww

4. Spirifer mesacostalis, Hall (?). (rr)
5. Liorhynchus globuliformis (Van.), Hall. (c)
6. Atrypa reticularis (Lin.), Dal. (r)
7. Phynchonella (Pugnax) pugnus (Martin), Day. (1)
Specimens rather small and poorly preserved, but pretty clearly

of this species.
8. Cyrtina Hamiltonensis, Hall. (rr)
9. Stropheodonta demissa (Con.), Hall. (rr)
10. Palwoneilo filosa (Con.), Hall. (c)
11. Palwoneilo ef. constricta (Con.), Hall. (rr)
One specimen better preserved approaches this species in mark-

ings and form,
12. Mytilarca carinata, Hall (?). (rr)
138. Schizodus cf. appressus (Con.), Hall. (r)
The specimens are nearer to figure 8, plate 75 (Palaeontology of
New York, Vol. V., Part [.), of the above species than to any other

form.

14. Lyriopecten cf. tricostatus (Van.), Hall. (rr)

A left valve that agrees quite well in its plications with
LI. macrodontus FH. of the Hamilton.
15. Actinopteria Boydi (Con.), Hall (?). (ar)
Crushed, but much like this species.
16. Crinoid segments. (a)
The Chenango Forks railroad station is at 901 feet, which makes the altitude
of the quarry approximately 964 feet A. T.

XXXVI A’. Near the top of the hill above A’ are loose. blocks of stone
containing plenty of specimens of Liorhynchus globuliformis (Van.), Hall, and
Rhynchonella (Camarotechia) Stevensi, Hall, which are probably from the
next fauna above that of the lower exposures at Chenango Forks. The
following species were noted in these loose blocks :

1. Liorhynchus globuliformis (Van.), Hall. (c)

2. Rhynchonella (Camarotechia) Stevensi (Hall), Hall and Clarke. — (ec)

3. Lehynchonella (Camarotechia) eximia (Mall), Hall and Clarke. (c)

It is probable that these specimens should be carefully com-
pared with /?. congregata (Con.), Hall, of the Hamilton, which

seems to be a closely allied species.

154 Report oF THE STATE GEOLOGIST.

4. Lyriopecten tricostatus (Van.), Hall (?). (rr)
The plications are of three sizes, giving the shell the surface
ornamentation of this species.
5. Palwoneilo, sp. (r)
Very poorly preserved.
6 Actinopteria cf. Theta, Hall. (rr)

Impertectly preserved, but like figure 19, plate 84 (Palaeontology

of New York, /oc. cit.) of this species.
This hill forms the divide between the Chenango and Tioughnioga rivers
above their junction, and its top is about two hundred and sixty-five feet

above the railroad.

Fenton and Chenango.

Greene is the southwestern township of Chenango county. To the south
is Fenton township, Broome county, which is on the eastern side of the
Chenango river, and on the western side of the river is Chenango township.

In the southern part of Fenton township is the small village of Port
Crane, formerly a port on the Chenango canal, but now reached by the
Susquehanna division of the Delaware and Hudson railroad, the station of
which is on the hill side, considerably higher than the village. The geology
of this region was a puzzle to Vanuxem, on account of the presence here of
Hamilton species. In describing the Chemung group, Vanuxem referred
to this difficulty and said: “These rocks appear [at Port Crane], having
similar fossils to those of the lower rocks which are quarried around the
village of Norwich, and those exposed in the sides of the brook to the west
of the village of Oneonta. There are three fossils at these localities also,
which are the same with those of the Hamilton group, the Posidonia lrata
| Paracyclas lirata (Con.), Hall], Strophomena carinata | Zropidoleptus cari-
natus (Con.), Hall], and Atrypa plebeia [this is not recognized]; showing
that localities existed which favored the continuance of certain species long
after their total destruction in others; a subject which requires thorough
investigation, and without which the value of fossils as a character will not
be as deservedly esteemed as they should.”’ Also, in describing the geology
of Broome county, Vanuxem mentioned the same difficulty and wrote:
“There are several openings in the hillside at Port Crane, not far from the
level of the canal, where some of the same fossils which exist at the quarries
near Norwich, and near the canal also, are found. These fossils belong to

1 Geology of New York, Part III., p. 180.

ProssER—HaAmILTON AND CHEMUNG SERIES. 155

the Hamilton group and, unless they have a high range, which I am disposed
to believe, would bring the Hamilton and the Chemung groups together in
two or more localities. They are anomalies which further observations are

required to explain or remove.” !

Vanuxem’s difficulty in reference to the
range of certain species in the vicinity of Port Crane and the bearing of the
above quotations will be appreciated after a description of the rocks exposed
near that village. At this locality the Chenango river makes a decided bend
to the west. On the eastern side of the river is a very steep hill and on the

western side a lower one.

ALIT A‘'. About a mile north of Port Crane exposures were found
from near the level of the canal extending for a considerable distance up the
hill. In the lowest rocks the following species were collected :

1. Lrorhynchus globuliformis, (Van.), Hall.

. (2) Lingula spatulata, Hall.

. Sphenotus rigidus (White and Whitfield), Hall (?).
4. Nucula corbuliformis, Hall (2).

5. (2) Goniophora, sp.

bo

Oo

In an old quarry near the village, C', quite an extensive fauna was
secured, as is shown by the following list :
“1. Rhynchonella (Camarotechia) eximia, Hall.
2. Spirifer, (2).
See S. mesacostalis with middle septum; H. 8S. W.
3. Spirifer sculptilis, Wall (?).
4. Spirifer granulosus (Con.), Hall and Clarke.
5. Chonetes setigera, Hall.
6. Chonetes scitula, Hall (2).
Wider forms than the common one, (. setigera, H.
Ambocelia umbonata (Con.), Hall.
Possibly this may be A. wmbonata var. gregaria, H.
8. Liopteria DeKayi, Hall (2).

There are two specimens and they are doubtfully referred to

a |

the above species.
9. Liopteria, sp. (small specimen).
10. Grammysia nodocostata, Hall.
11. Grammysia subarcuata, Hall.

1 Geology of New York, Part III., pp. 294-295.

156 Report OF THE SratE GEOLOGIST.

12. Modiomorpha mytiloides (Con.), Hall.

Two specimens are rather short, in this respect resembling J.
alta (Con.), H., but their umbonal slope is not sharp enough for
that species. Another specimen is much elongated and very
ventricose along the region of the umbonal slope.

13. Modiomorpha macilenta, Hall (2).
14. Microdon (Cypricardella) bellistriatus, Con.
15. Paleoneilo plana, Hall.

ji
for)

. Leptodesma, sp.

i
~]

. Small lamellibranch shell, possibly Modiomorpha.

pi
2

Goniophora, sp.

an
ie)

Sphenotus, sp.

=

Coleolus tenuicinctum, Hall.

ed

Bellerophon, sp.

bo

Cyclonema multilira, Hall.
Loxonema Hamiltonie, Hall.
Pleurotomaria Itys, Hall.
5. Orthoceras, sp. (fragments).
ALIT 4. About one and one-half miles southwest of Port Crane a
section was made extending from the canal level to the top of the high hill.

co

t

bo bb Ww WH WH Ww

At the base of the hill, only a few feet above the river and canal level, are
olive, argillaceous shales in which fossils are rare, Spirifer mesastrialis, Hall,
and Rhynchonella (Camarotechia) Stevensi, Hall (2), being the most common
species. The complete list is:
1. Spirifer mesastrialis, Hall. (c)
Mostly broken specimens, but they show clearly the fine striae
on the plications and sinus.
2. Spirifer mesacostalis, Hall. (rr)
The type of S. aewminata, Hall, 1843. Another specimen seemed
to be similar, but it has very fine striae on the plications, like
S. mesastrialis.

3. Tropidoleptus carinatus (Con.), Hall. (rr)
4. I?hynchonella (Camarotechia), Stevensi (H.), H. and C. (ce)
5. Chonetes setigera, Hall (2). (rr)

Imperfectly preserved, with thirty to forty striae.
6, Modiomorpha subalata (Con.), Hall, var, Chemungensis,
Hall (2). (1r)

Not clearly preserved.

CHEMUNG,

SECTLON V2 MULES SOUTA-WEST
OE LOR CRONE
(+42 8)

1440 ON, Xpprox :

590° b opr OF AL Vn Second aa.
& wei Sandstones Whit x

SPIRIPER, WIESASTRIQUS
Abundant,

- Chin Sandstone.
S SPLAACER, MS Suroreus ,

a Whosi\y ive Sholes,

RR. revel Orypros. \o4y ON,

Bwash Shaky Sandstone.
TROIRLOOLEELUS CARIMQATUS.
———$——— Bluish Shales Qua Thin

= |6 Soandstones

—————— x O\ive Shares.

a SPIRIEER THESOSTRIQAS
Chenongo Ravers Level, Qpprox M6 AN,

157

—

8 |

158 Report oF THE STATE GEOLOGIST.

7. Paleoneilo brevis, Hall (2). (ir)
8. Palwoneilo plana, Hall (?). (ar)
9. Schizodus cf. appressus (Con.), Hall. (rr)

In form similar to figure 8, of plate LXXV (Palaeontology of
New York, /oc. cit.), which is described as “a small right valve of
rotund form.”

NLIT 5. About eighty feet above the river level on the very steep
hillside is a small excavation in bluish shales and shaly sandstones. Fossils
are somewhat abundant, the most common species being Microdon (Cypri-
cardella) complanatus, Hall, and Palwoneilo constricta, (Con.), Hall. The

following species were obtained :

1. Spirifer mesastrialis, Hall. (ar)
2. Microdon (Cypricardella) complanatus, Hall. (a)
3. Microdon (Cypricardella) gregarius, Tall. (rr)
4. Palwoneilo constricta (Con.), Hall. (c)

The specimens are external impressions of poorly preserved
shells, but they agree closely in form and general appearance with
figure 1 of this species on plate XLVIII (Palaeontology of New
York, Joc. cit.).

5. Nucula corbuliformis, Hall. (rr)
Form and proportions agree well with those of this species.
6. Paracyclas (2) pauper, Hall (¢). (r)
The specimens are not sufficiently well preserved to show much
of the markings, but they seem to agree more nearly with the
figures of this species than with those of any other,
7. Palwoneilo plana, Hall. (rr)
8. Bellerophon, sp. (ar)
This may be compared with 4. Mera, H., of the Chemung, but
it is so poorly preserved that it is difficult to determine.
9. Fragment of Bryozoa. (rr)
10. (4) Edmondia, sp. (rT)

XLII 6°. In the slope somewhat above the quarry in bluish shaly
sandstones, fossils are common, as the list indicates :
1. Tropidoleptus carinatus (Con.), Hall. (7)
2. Rhyncnonella (Camarotachia) ecimia (H.), Hall and Clarke. (a)
See “2. Stevensi (H.), H. and C. The smaller specimens have
proportions nearer those of &. eximia, while the larger are more
like 2. Stevensi.

ProssER—HAmMInToN AND CuHEMUNG SERIES. 159

3. Spirifer mesacostalis, Hall. (c)

One ventral impression distinctly shows the median plication
which is supposed to define this species. Another specimen is
almost the same as figure 3, plate XL, Pal. I'V., except that it shows
a distinct smus on the fold. This form was originally described as
S. acuminata which, m Vol. VIIL., IL. is stated to be probably
S. mucronatus (Con.), Bill., var. posterus, H. and C. It it pos-
sible that some of these specimens belong to this species, but they
all clearly show a sinus on the fold, or fold in the sinus, which is

characteristic of S. mesacostalis.

4. Ambocelia wmbonata (Con.), Hall. (c)
5. Chonetes setigera, Hall (2). (1)
6. Microdon (Cypricardella) gregarius, Hall. (c)

XLIIT &B. Exposures in the cuts along the Delaware and Hudson
railroad, 175 feet above the river level. The rocks are mostly olive shales,
but there are some of a bluish color that are iron stained and these contain
most of the fossils; interbedded are thin shaly sandstones. /?hynchonella
(Camarotechia) Stevensi, Hall; Spirifer mesacostalis, Hall, and Microdon
(Cypricardella) gregarius, Hall, are the most common species. The list is as
follows :

1. Rhynchonella (Camarotechia) Stevensi (H.), Hall and Clarke. (a)

Some of the specimens may be compared with /?. eximia (H1.),
H. and C., as they are broad and similar in outline.
2. Spirifer mesacostalis, Hall. (a)
The impressions of two ventral valves show very distinctly the
median septum in the sinus.

3. Spirifer mesastrialis, Hall (?). (17)

A large specimen with twenty or more plications on each side

of the sinus.

4 Ambocelia umbonata (Con.), Hall. (ir)
5. Chonetes setigera, Hall. (rr)
6. Microdon (Cypricardella) gregarius, Hall. (a)
7. Microdon (Cypricardella) complanatus, Hall (?). )

A few specimens are not dissimilar to figure 23, plate LXXIII
(Palaeontology of New York, /oc. cit.), of M. tenwistriata and
perhaps should be referred to that species.

8. Orthoceras, sp. (fragments). (ar)

160 REPORT OF THE STATE GEOLOGIST.

9. Leptodesma cf. sociale, Hall. (rr)
The specimens do not show the strong concentric markings of
this species, but fine striae as in L. Pogersi, Hall, to which species
perhaps they should be referred. The form is similar to that of
the small specimens of LZ. Rogerst or L. sociale.

XLIT Bb. By the roadside at the top of the hill above the railroad
are thin, very much weathered sandstones that contain fossils. The following
were collected :

1. Spirifer mesastrialis, Hall.

Dy Spirifer disjunctus, Sowerby.

3. (4) Aviculopecten, sp. .

4. Crinoid segments.

This is the first place in the Chenango valley where Spirifer disjunctus
was found, and the occurrence of this characteristic Chemung fossil conclu-
sively proves that the rocks near the top of the high hill south of Port Crane
are in the Chemung formation.

LB. On top of the high hill along the second road south of the river,
and about two miles south of Port Crane, are thin sandstones in which
Spirifer mesastrialis, Hall, is abundant. There is only a slight exposure by

the roadside, but the following species were collected :

1. Spirifer mesastrialis, Hall. (a)
2. Mytilarca carinata, Hall. (rr)
3. Paleoneilo, sp. (rr)

An elongated specimen which is narrower than any of the
figured forms.

4. (2) Schizodus, sp. (rr)

5. Crinoid segments. (a)

This fauna is about 590 feet above the river level or with an approximate
altitude of 1,440 feet A. T., and it is in the highest rocks found in the vicinity
of Port Crane.

XLIITI A. Two miles east of Port Crane is Osborne Hollow, in the
western part of Colesville township. The railroad station is 1,115 feet A. T.
The country about this place is gently rolling, with few extensive rock
exposures. The species in the following list were obtained from an outcrop
along the brook near the village:

1. Modiomorpha, sp.

2. Leptodesma, sy.

3. Microdon (Cypricardella) bellistriatus, Con., var.

ProssER—H Am ILTON AND CHEMUNG SERIES. 16]

4. Spirifer mesacostalis, Hall (¢).
5. Spirifer mesastrialis, Hall.
6. Phynchonella (Camarotechia) Stevensi, Hall.
7. Productella, sp.
8. Paleoneilo constricta (Con.), Hall (%).
9. Palewoneilo plana, Hall (2).
10. (2) Paleoneilo, sp.
11. Schizodus gregarius, Hall.
12. Nuculites, sp.
13. Liopteria Rafinesquii, Hall.
14 Liopteria Bigsbyi, Hall.
15. Grammysia bisulcata (Con.), Hall.
16. Goniophora Chemungensis (Van.), Hall.
17. (2) Sphenotus, sp.
18. Chonetes scitula, Hall (?).
19. Chonetes setigera, Hall.
20. Chonetes, sp.
21. Crinoid stem and segments.
22. Plant stems.
23. Platyceras.
24. Coral remains
XIIII B. Some years ago three shafts were sunk to quite a depth,
near the village, in search of galena. From the rocks remaining on the dump
heaps of these shafts the species enumerated below were collected :
1. Tropidoleptus carinatus (Con.), Hall.
2. (2) Rhynchonella, sp
3, Bryozoa.
4. Rhynchonella (Camarotachia) Stevens’, Hall.
5. Spirifer mesacostalis, Hall (2).
6. Grammysia bisulcata (Con.), Hall.
7. Nucula, sp.
8. Sphenotus, sp.
9. Lnopteria, sp.
10. Chonetes scitula, Hall (?).
11. Leptodesma, sp.
12. Microdon (Cypricardella) gregarius, Hall.
13. Paleoneilo, sp.
14. (2?) Goniophora Chemungensis (Van.), Hall.
Tt

162 Report oF THE State GEOLOGIST.

15. Loxonema delphicola, Hall.
16. Crinoid segments.
17. Fragments of fish bones like Ho/onema rugosa (Claypole), Newb.
XLII 1", On the hillside west of the Chenango river, opposite Port
Crane, is an old quarry that was opened during the construction of the
Chenango canal. It is in the eastern part of Chenango township, and the
bottom is some seventy-five or more feet above the river. The wall of the
quarry shows fifteen feet of bluish shales and shaly sandstones that weather
to an olive color, Some of the thin sandstones and slightly calcareous layers
contain fossils abundantly, especially /?hynchonella (Camarotechia) Stevensi,
Hall, and Zropidoleptus carinatus (Con.), Hall. The species in the list were
gathered in one half hour:
1. Zropidoleptus carinatus (Con.), Hall. (aa)
Typical specimens of this species such as occur in the Hamilton.
2. Lhynchonella (Camarotechia) Stevensi (H.), Hall and Clarke (#). (aa)
The ventral valves of a number of specimens show clearly the
dental lamelle described in this species, and the dorsal valves, the
septum about one-third the length of the shell. However, the
plications are less than given for this species, and in form many of
them are about the same as /. eximia with which they must be
compared.
3. Chonetes scitula, Hall. (rr)
One specimen shows over fifty striae and is clearly of the form

of this species.

4. Orthonota (?) parvula, Hall. (7)
5. Microdon (Cypricardella) gregarius, Hall. (c)
6. Paleonetilo plana, Hall (2). ar)
7. Goniophora, ct. Chemungensis, (Van.), Hall. (rr)
8. Grammysia elliptica, Hall (?). (rr)

Imnperfectly preserved.
9. Grammysia circularis, Hall. (rr)
The posterior portion of the shell is not complete, but in all the

characters preserved it agrees well with this species.

10. Crinoid stems and segments. (c)
11. Liopteria De Kay, Hall (?). (c)

The specimens resemble quite closely figure 6, plate LX XXVIII

(Pal., N. Y.), which is a large specimen from Schoharie county.

ProssER—HAMILTON AND CHEMUNG SERIES. 163

XLIT FE. Along the bank of the Chenango river, about two and one-
half miles below Chenango Forks and opposite Kattle Hill, are quite fossil-
iferous shales. There is one layer that is quite calcareous, forming a “fire
stone,” which contained these species :

1. Spiriter mesacostalis, Hall (2).
2. Productella speciosa, Hall (Ithaca variety).
3. Fehynchonella (Pugnaax) pugnus (Martin), Dav.
4. Liorhynchus globuliformis (Van.), Hall.
5. Cyrtina Hamiltonensis, Hall.
6. Crama (Craniela) Haniltonie, Hall (2).
The shales contained the succeeding :

i

. Orthis (Schizophoria) impressa, Hall.
2. Liorhynchus globuliformis, (Van.), Hall.
3. Spirifer mesacostalis, Hall (2).
4. Stropheodonta demissa (Con.), Hall.
5. FRhynchonella (Camarotechia) Stevensi, Hall.
6. Productella speciosa, Hall.
7. Paleoneilo constricta (Con.), Hall (?).
8. Lyriopecten tricostatus (Van.), Hall.

9. Microdon (Cypricardella) bellistriatus, Con. (?).

10. Sphenotus, sp.

Liorhynchus globuliformis (Van.), Halli, is the most abundant species in
both of the preceding lists.

ALIT H*. Two miles below Chenango Forks is a long cut on the
Delaware, Lackawanna and Western railroad, furnishing a good locality to
atudy the Lvorhynchus globuliformis fauna. The rocks are principally
sandstones and shales which, on weathering, are of an olive color. Above the
railroad cut is the highway along the steep eastern face of Kattle Hill, where
the rocks are not very fossiliferous except in thin layers. These layers are
somewhat calcareous, often at the bottom of a four to six inch sandstone, and
contain a mass of fossils, principally Liorhynchus globuliformis (Van.), Hall,
mixed with a few other species. This Zéorhynchus, under the name of
Atrypa globuliformis, was figured by Vanuxem, who said: “This cast is
given, because it exists in myriads as such in this group [the Chemung |,
numerous localities abounding in it.”' Professor H. 8. Williams has termed
this horizon “the Liorhynchus globuliformis stage” of the faunas succeeding

the Oneonta formation in the Chenango valley.’

1 Geology of New York, Part TIL, p. 182 See fig. 2 of No. 49 on same page.
2 Proceedings American Association Advancement of Science, Vol. XXXIV., 1886, p. 226.

164 Report oF THE STateE GEOLOGIST.

To indicate the base of the Chemung formation across Chenango and
Otsego counties is a matter of some difficulty. There is a difference of
opinion among working geologists as to where it occurs in this region, and
possibly as yet insufficient study has been given to these higher rocks to
enable the determination of this point. Vanuxem’s interpretation of this
region is of little value on account of his failure to separate the Oneonta
from the Catskill formation, as will be seen by reference to the Geological
Map of the State of New York, of 1842. Professor James Hall has given
careful attention to the classification of these rocks and mentioned them in
numerous publications, among which might be cited his paper before the
National Academy of Sciences, in which he clearly stated his interpretation
when he said: “The fossilferous beds of the Chemung are found lying upon
that formation [the Oneonta} between Norwich and Oneonta, and to the east
of Sidney Plains, and at or near Franklin, where they apparently pass
beneath the great red- sandstone formation of the Catskills.”' Professor
Henry S$. Williams placed the base of the Chemung considerably higher,
beginning above the Zropidoleptus carinatus fauna near Port Crane,
apparently with the Spirifer mesastrialis zone well toward the top of the
hill south of Port Crane? Mr, Darton evidently followed Professor Hall’s
classification and stated that: “From Franklin, westward, the Oneonta-
Chemung boundary is clearly marked by the abrupt change from red beds to
grey shales and soft sandstones.”? Finally, Professor Clarke, as a result of
his studies in the vicinity of Greene, concluded that the fossils in the shales
and sandstones overlying the Oneonta formation “are of typical Chemung
expression,” * and consequently referred the rocks to the Chemung formation.

Professor Williams described the lowest Chemung fauna of the Cayuga
lake meridian as found on the high hill south of Ithaca in Danby township
in the southern part of Tompkins county “stratigraphically 1,300 feet or
more above the Genesee shale”> The following fauna from this locality is
given by Professor Willams:

“ Productella lachrymosa,

Ambocelia wmbonata var. gregaria,

Orthis impressa (second variety, wide and large),

Atrypa reticularis,

and a few other imperfect fossils.” °

1 Science (old series), Vol I., Dec. 11, 1880, p. 290.

2 Proceedings American Association Advancement of Science, Vol. XXXIYV., section IX. of Chart.
3 American Journal of Science, third series, Vol. XLV., 1893, p. 207.

4 Thirteenth Annual Report State Geologist [New York] , p. 543; also see section on p. 556.

5 Bulletin United States Geological Survey, No. 3, 1884, p. 21.

6 Tbid., p. 21.

- f
HAMILTON AND CuEMUNG SERIES. 165

Prosser

It will be noticed that in the above fauna Spirifer disjunctus, Sow., is
not reported ; but above the fauna just cited occur shales that contain a fauna
“very similar to that in the dark shale at the base of the Ithaca group, but

mingled with other species. The most northern exposure, at which

the typical Chemung fauna was found in abundance, was high up in the hills

ela

in the northeastern part of Chemung county, near Park station,” ' and at this
place Spirifer disjunctus, Sow., and Orthis Tioga, Hall, were found, some
300 or 400 feet stratigraphically above the lowest fauna in Danby.

On comparing the list of fossils reported by Professor Williams from the
lowest Chemung in Danby? with the list given by Professor Clarke for
Greene, or the fauna reported in this paper from Chenango Forks, it will be
seen that all the species listed by Professor Williams from Danby, except
Ambocelia umbonata var. gregaria, occur in these localities in Chenango
county. Again it will be found that the thickness of the formations from the
top of the Genesee slates to the base of the fauna overlying the Oneonta of
the Chenango valley, and the similar fauna above the Upper Portage of the
Cayuga lake region is about the same. Professor Williams reports it as
“1,300 feet or more” * for Tompkins county, and in the Chenango valley it is
fully 1,300 feet from the top of the Hamilton to the base of the fauna imme-
diately above the Oneonta formation. Finally Professor Williams described
a fauna containing Zropidoleptus carinatus* near Owego” at about the same
altitude as the Zropidoleptus carinatus zone near Port Crane, which is in the
midst of a typical Chemung fauna, at least 200 feet above the first occurrence
of Spirifer disjunctus, Sow. It is thought that possibly the Owego zone of
Tropidoleptus represents the same general part of the section as that at Port
Crane, except that the Zropidoleptus fauna is being replaced by the regular
Chemung fauna near Owego, consequently it is not so conspicuous as in the
sections farther east.

After reviewing the results obtained by different investigators of this
problem of the separation of the Chemung and Portage and the Chemung
and Oneonta formations in the central part of southern New York, the facts
seem to justify the conclusion that the Chemung begins with the Orthis
impressa fauna overlying the Oneonta formation.

The thickness of the formations composing the Chenango valley section,

ranging from the base of the Marcellus shale in Sangertield township, Oneida
1 Bulletin United States Geological Survey, No. 3, 1884, p. 22.
2 [bid., p. 21. .
3 Thirteenth Annual Report State Geologist [New York], p. 543.
4 Bulletin United States Geological Survey, No. 3, p. 21.
5 Ibid., p. 24.

166 Report or rie SraTE GEOLOGIST.
county, up into the Chemung on top of the high hill in Fenton and Kirkwood
townships, Broome county, to the northeast of Binghamton, is approximately
as follows: estimating the dip for the northern part of the Chenango valley
to be sixty feet to the mile, we would have a thickness of about 1,500 feet for
the Marcellus and Hamilton formations. To the east of Smyrna there are,
perhaps, twenty-five feet representing the Tully limestone and Genesee slate.
The Sherburne formation is 250 feet, the Ithaca 500 feet, or more, and the
Oneonta 550 feet thick; while for the Chemung from Greene to the top of
the hill south of Port Crane, calling the dip 60 feet per mile, there are 1,225
feet, which result agrees quite well with the record of the well drilled at
Binghamton."

The thickness of these formations may be more clearly and concisely
expressed in tabular form, as shown on the accompanying generalized section

of the Chenango valley.

Tuer Unapmia VALLEY SEcrTION.

The courses of the Chenango and the first river to the east, the Unadilla,
are approximately parallel, and are, on the average, ten miles apart. For a
considerable distance the Unadilla river serves as the dividing line between
Chenango and Otsego counties. The general topographic features of the

two valleys are very similar, and they cross the same formations.

Columbus.

Columbus is the northeastern township of Chenango county, being
directly east of Sherburne, south of Brookfield, Madison county, and sepa-
rated by the Unadilla river on the east from Edmeston, Otsego county,
In describing the exposures of this township, we begin with those directly
east of the outcrops described near Harrisville, Sherburne township and, con-
tinuing eastward, follow somewhat closely the line of separation between
the Hamilton and Sherburne formations.

ALIX £*. Kast of Harrisville, along the main road from Sherburne to
Columbus, are occasional outcrops. By the roadside, on the divide at the
head of Mad brook, are shaly layers containing fossils; Liorhynchus mesa-
costalis, Hall, being abundant, while Productella speciosa, Hall (?), and
Cyrtina Hamiltonensis, Hall, are common. The locality is Just east of the
Sherburne and Columbus township line, about two miles east of Harrisville,

fo)

and barometrically 485 feet higher than the lower reservoir dam at Harris-

1 Bulletin Geological Society of America, Vol. IV , pp. 93, 94.

CEXERQUZED SECTION QHUIAG
TRAIOAUESS OF TRE CHENAGG
VOLE, EORMOTIONS,

4050

CAEN, To he Top OF
The ML OW Royt Crane.

2825

OVE OWT.

AW ROACH,

SHERRURAE
GEVES ER Oma KWUOULL
25 Feet Whrick Aa

WOMEN

Oud

WOARCEULAS .

168 REpoRT OF THE STATE GEOLOGIST.

ville, or approximately 725 feet above the railroad level in Sherburne village,
which makes its altitude about 1,767 feet A. T. This outcrop belongs in the

Ithaca formation. A rather hasty search revealed the following fossils :

1. Liorhynchus mesacostalis, Hall. (a)
2. Spiriter granulosus (Con.), Hall (2). (rr)
3. Spiriter, probably Sp. mucronatus (Con.), Bill. (rr)
4. Cyrtina Hamiltonensis, Hall. ; (c)
5. Chonetes scitula, Hall. (rr)
6. Productella speciosa, Hall (?). (c)
Very similar to specimens identified as this species at Ithaca.
7. Nucula corbulitormis, Hall. (ir)

NIX J. At the corner of the second east and west road, north of the
Sherburne and Columbus turnpike, and one and one-half miles northwest of
XIX BS, is the head of the northeast branch of Mad brook. Beginning
immediately below the road, and appearing at intervals down the brook, are
blackish shales containing abundant fossils. An anticlinal roll crosses the
brook some distance below the road. These shales are on the Andrews farm,
two miles northeast of the Sherburne reservoir at Harrisville, and the upper
part of them is some 590 feet above the railroad at Sherburne. The abundant
fossils are all Hamilton species, and the shales are apparently in the upper

part of the Hamilton formation. The following species were obtained :

1. Spirifer mucronatus (Con.), Bill. (a)
2. Spiriter granulosus (Con.), Hall. (c)
3. Spirifer Tullius, Hall. (rr)
4. Vitulina pustulosa, Hall. (17)
5. Tropidoleptus carinatus (Con.), Hall. (c)
6. Chonetes scitula, Hall. (c)

These resemble somewhat ( setigera, H., but are probably rather

short forms of the above.

7. Lingula punctata, Hall. (r)
8. Vucula corbuliformis, Hall. ar)
9. Palawoneilo maxima (Con.), Hall (7). (ar)
10, Liopteria, sp. (ar)
Ll. Dalmanites (Cryphwus) Bootht (Green), Hall. (Vr)
12. Phacops rana (Green), Hall. (rr)

On the hill south of the creek and 150 feet higher, are arenaceous iron-

stained shales that contain an occasional small lamellibranch and Liorhynchus.

ProssER—HAMILTON AND CHEMUNG SERIES. 169

Interstratitied with the shales are also thin, smooth sandstones. The rocks
probably belong in the Sherburne formation.

On the first road turning to the east about one-fourth of a mile north of
the Andrews farm and eighty-five feet above the Hamilton shales at XIX D',
are fine bluish, argillaceous shales which belong in the Sherburne formation.
These shales form the upper part of the northern end of the steep hill along
the Sherburne and Columbus township line. On the eastern side of the steep
hill, fossils were found about seventy feet below the exposure of the Sherburne
shales, just described, which are regarded as near the top of the Hamilton.
This outcrop is about 600 feet above the railroad level at Sherburne or approx-
imately 1,642 feet A. T.

NIX FE. Ina branch of Howard creek, at the foot of this hill, is a blue
sandstone, above which are coarse arenaceous shales. The outcrop is on the
Thomas Mulligan farm, three miles northwest of Columbus village, and is 155
feet lower than the stratum with fossils on the hillside, or approximately 1,487
feet A. T. The shales are blocky, split into irregular pieces, and contain
plenty of Hamilton fossils. The following species were collected :

1. Tropidoleptus carinatus (Con.), Hall. (c)
2. Orthis, sp. (rr)
3. Spiriter granulosus (Con.), Hall. (r)
4. Orthothetes Chemungensis (Con.), H., var. arctostriata, H. (rr)
5. Microdon (Cypricardella) tenuistriatus, Hall. (r)
6. Pholadella radiata (Con.), Hall. (rr)
7. Nucula bellistriata (Con.), Hall. (1r)
8. Grammysia bisulcata (Con.), Hall. (rr)
9. Grammysia ct. G. alveata (Con.), Hall. (11)

10. Coleolus tenuicinctum, Hall. (17)

11. Cyclonema multistriata, Hall (?).

12. Leptodesma, sp. (rr)

AIX F', At the foot of a small glen one and two-tenths miles south-
west of the above exposure, are coarse arenaceous shales, containing plenty
of Hamilton fossils. Then, for about twenty feet, the rocks are covered, while
in the glen above is an excellent exposure of the Sherburne shales and sand-
stones (F*). The glen is cut out of rocks belonging to this formation, and on
the road above, in front of Mr. Pultz’s house, the thin argillaceous shales
are ‘well exposed. This locality is but a short distance east of the Sher-
burne and Columbus township line, and 150 feet of the Sherburne formation

are shown.

170 Report or THE Srare GEonocisr.

New Berlin.

New Berlin township is directly south of Columbus, its eastern boundary
being the Unadilla river, its western Norwich and North Norwich, while
Sherburne forms a part of its northern boundary. West brook rises in the
southern part of Columbus and flows southeasterly across the northeastern
part of New Berlin and through New Berlin village into the Unadilla river.
In the southwestern corner of Columbus, to the northwest of the head of
West brook, is the high divide which runs north and south along the Sher-
burne-Columbus township line and for some distance south into New Berlin.
On top of this divide in the southwestern part of Columbus, are the rocks
(XIX C*) which were referred to the Ithaca formation when describing the
exposures along “ Nigger brook” in Sherburne township.’

XX A‘ Commencing about one-half of a mile east of XIX C4, are
exposures of rocks, and at intervals there are small outcrops for one and one-
half miles along the highway to the southeast when the upper part of West
brook is reached. Along the brook there are plenty of exposures from near
its head to New Berlin village. The exposure A! consists of arenaceous shales
by the side of the highway nearly five miles northwest of New Berlin village.
This outcrop is 670 feet higher than the New Berlin railroad station, or
approximately 1,758 feet A. T. Only a few minutes were spent in collecting
fossils, but a number of species were obtained, among which occurs Spirifer
mesastrialis, H. The fauna and stratigraphic position of the layer show it
to be in the Ithaca formation. Below is the complete list of fossils :

1. Spirifer mucronatus (Con.), Bill., var. posterus, H. and C. — (c)

One of these specimens is quite like the form of S. mesacostalis,
H. (as figure 10 plate 40, Palaeontolgy of New York, Vol. IV.).

2. Spirifer mesastrialis, Hall. (rr)
3. Chonetes scitula, Hall. (c)
4. Eehynchonella (Camarotaechia) eximia, Hall (2). (rr)
5. Liorhynchus mesacostalis, Hall. (rr)
6. Atrypa reticularis (Linné), Dalm. (ar)
7. Stropheodonta demissa (Con.), Hall. (r)
8. Actinopteria, sp. (rr)
9. Grammysia ct. elliptica, Fall. (rr)

XX A’. About three-fourths of a mile southeast of the locality just
described, near the head of West brook and 180 feet lower, fossiliferous are-

2 On profile N. Y., O. & W. railroad New Berlin is given as 1,088 feet.

ProssER—Hamintton anp CuEemunG SeErtes. 171
1. Spirifer mucronatus (Con.), Bill., var. posterus, H. and C. (1)
2. Liorhynchus mesacostalis, Hall (2). (1r)
3. Modiomorpha ct. subalata (Con.), Hall. (rr)

No umbonal ridge is shown and so it departs from the form of
this species. The umbonal slope being rounded, the specimen may
belong to the genus L’/ymella.

On the hillside, eighty feet above the road, are thin, apparently unfos-
siliferous sandstones (A°), These two exposures are in the Ithaca formation,

XX A‘. One hundred feet lower than A°, thin, micaceous sandstones
alternating with shales, are well exposed along West brook. The surface of the
thin sandstones is usually shiny, but some specimens have a glazed, blackish
surface in which specimens of Hucotdes graphica, Van., occur. ‘These rocks
are in the Sherburne formation, the top of which is probably not much above
this outcrop. This ledge is 390 feet above the railroad station in New Berlin,
or approximately 1,478 feet A. T. The thickness of the rocks from this out-
crop down to the top of the Hamilton formation, as exposed on the banks of
West brook in the edge of New Berlin village, is 255 feet, which is approxi-
mately the thickness that we have assigned to the Sherburne formation of
Chenango county. Farther down the brook and some seventy feet lower is a
rocky glen which gives an excellent idea of the Sherburne shales. The rocks
are mostly bluish or blackish shales, forming steep banks on each side of the
brook, with only sufficient space between them for the stream and highway.
This formation continues down the brook into the edge of New Berlin village.

XX A*. The base of the Sherburne formation occurs in West brook at
the beginning of the former mill race and upper dam, just above the old
brewery. This locality is now on the farm of Thomas Lowe, at which place
the thin, bluish-grey, smooth sandstones and shale of the Sherburne formation
are clearly shown resting directly on the bluish-black, coarser arenaceous
shales of the Hamilton. There is apparently no representation of charac-
teristic Tully limestone and Genesee slate. Fossils appear in the Hamilton
shales just below the dam and, a little lower, the creek has cut a narrow
gorge through these rocks with walls from twenty to twenty-five feet high.
The top of the Hamilton is about 185 feet above the railroad level at New
Berlin station, or approximately 1,223 feet A.'T. These upper shales of the
Hamilton are quite fossiliferous, but the number of species is small. The
following were found in the shales just below the dam and above the gorge:

1. Spirifer mucronatus, (Con.), Bill. (c)

2. Spiriter Tullius, Hall. (c)

SELTAOTA QUOTUG, WEST BRO AQ
AVATAER TED BEAU QA SMOUTAERY

IBZ ONT. Qypros, CYROMBUS. G20. 0)

— Qn Divide eee West : Se

0) ae AYAATH Shales.

Wiostly Covered.
iin Sandstones.

AUN WOCR |

Vovered .

SURABOARME Ln < ey Vast 04
\) est By iN) ok

Povily, Covered.
Gorge Lo SARA P

Ravi ly, Covered.

NY SALRAUAMR, Shales.

we WOKUTON Sonadclones Quad
Shales On West Brook
2 Quad West Street.

RALevel OX New Berlin, 1088 ON,

172

ProssErR—Haminron AND CHEMUNG SERIES. L73

3. Leptodesma Rogersi, Hall (4). . (c)

Rather imperfectly preserved, but more like this than any other
fossil figured.

XX A*. In the lower part of the gorge of West brook in New Berlin
village are coarse arenaceous shales alternating with those that are somewhat
argillaceous. This exposure begins in the brook only a few rods above the
Eagle hotel and about fifty feet above the railroad level. These upper
Hamilton rocks are excellently shown in this gorge of West brook along West
street in New Berlin village. Fossils are very abundant in layers, the fol-
lowing list giving a good idea of the fauna of this part of the formation :

1. Spirifer audaculus (Con.), Hall (2).
It is possible that these specimens are all S. granulosus (Con.),
Hall. The surface markings are not preserved and they are largely

internal impressions.

2. Spirifer granulosus (Con.), Hall. (c)
3. Spiriter mucronatus, (Con.), Bill. (1r)
4. Atrypa reticularis (Linné), Dalm. (Gag)
5. Tropidoleptus carinatus (Con.), Hall. (ar)
6. Nucula lirata (Con.), Hall. (rr)
“7. Modiomorpha mytiloides (Con.), Hall. . ar)
8. Ambocelia wmbonata (Con.), Hall. (11)
9. Chonetes coronata (Con.), Hall. (rr)
10. Palwoneilo constricta (Con.), Hall. (1)
11. Pleurotomaria capillaria, Con. (rr)
12. Spirophyton velum (Van.), Hall (2). (rr)

XX F'. A brook enters the Unadilla river from the west, one and one-
fifth miles south of New Berlin village, which affords a good exposure of the
rocks just west of the river road. The lowest rocks, which are coarse, are-
naceous shales containing an abundance of Hamilton species, form a small
fall, above which is a short gorge and second fall. The fauna is as follows:

1. Spirifer mucronatus (Con.), Bill. (a)

Typical mucronate forms of this species as in figure 15, plate 34,

Vol. IV, Palaeontology of New York.

2. Tropidoleptus carinatus (Con.), Hall. ar)
3. Spirifer granulosus (Con.), Hall. (rr)

Or S. audaculus (Con.), H. Very much weathered external im-

pressions.

174 Report oF THE STATE GEOLOGIST.

4. Spiriter Tullius, Hall (2). (c)

Form of this species, but not well enough preserved to show the
fine striae.

5. Leptodesma Rogers, Hall. (1r)

XX 6. Less than five feet above the top of the first fall are blue
shales alternating with thin sandstones which form the rocky sides of the
narrow gorge. These rocks have the typical lithologic characters of the
Sherburne, and from their stratigraphic position undoubtedly belong at the
base of that formation. This is one of the best localities found in the Una-
dilla valley for the purpose of illustrating the transition from the Hamilton
to the Sherburne formation. It indicates that the conditions under which the
Tully limestone and Genesee slate were formed had nearly ceased and that
the lithologic characters of those formations are scarcely represented in the
Unadilla valley. Vanuxem mentioned the occurrence of the Genesee slate at
North New Berlin (now New Berlin) *, but it was probably some of the rather
darker shales of the Sherburne which he considered the Genesee, and, in fact,
under his description of the formation it is stated that “The Genesee slate was
not distinctly recognized east of the town of Smyrna in Chenango county.” ?

Fossils are very rare in these shales, only two fragments of a Gonéatites
and another of a different shell bemg found. In this glen the top of the
Hamilton, according to barometric readings, is approximately 140 feet lower
than it is at XX A®, in West brook, New Berlin village, scarcely two miles
farther north, which would give, approximately, a dip to the south of seventy
feet per mile. Although this dip is considerably greater than former esti-
mates, still it agrees closely with the estimates in the earler part of this
report for the exposures ten miles farther west along the Chenango valley.
The base of the Marcellus shale is north of Bridgewater in the upper part of
the Unadilla valley, twenty miles north of XX B, and, providing the dip is
as great for the entire distance as in the vicinity of New Berlin, we would
have a thickness along the Unadilla valley of over 1,300 feet for the Marcellus
and Hamilton formations. The lithologic characters and fauna of the Hamil-
ton and Marcellus formations as shown along the Unadilla river valley from
New Berlin to Bridgewater have been described in a former paper.® About
one mile south of XX B is a smaller brook which exposes shales and thin

sandstones of the Sherburne formation.

1 Geology of New York, Part III., p. 292.

2 Thid., p. 169.

3 Prosser: The Devonian section of centrai New York along the Unadilla river. Twelfth Annual Report State Geologist
[New York], 1893, pp. 110-142.

ProssER—HaAminton AND CHEMUNG SERIES. 175

XX ©. About three and one-fourth miles south of New Berlin is the
small hamlet of New Berlin Center. To the west of the Unadilla is a steep
hill which rises between 400 and 500 feet above the river level. This hill
was studied north of New Berlin Center and opposite the schoolhouse of
District No. 4.

SECTION OF XX C, NORTH OF NEW BERLIN CENTER.

SU | Brow of hill.
130’ | Thin sandstones and arenaceous shales. J/thaca.

OTA C2.

162’ |= Sherburne.

FS) =| aac _C. Fine blue shales.
37° Covered.

0 a eee Railroad level.

15’ | Covered.

(eae River level.

As the above section shows, the valley and lower part of the hill do not
exhibit outcrops of rocks, but at C', fifty-two feet above the river, is a small
exposure of thin blue shales which clearly belong in the Sherburne formation.
Its base is probably below the bed of the river at this locality and the for.

mation continues for about 214 feet up the hillside.

XN OC? At 214 feet above the river level the rocks are coarser and con-
sist of thin sandstones with arenaceous shales, the lower part containing but
few fossils, which increase in abundance in the higher layers. These shales
and sandstones are in the Ithaca formation, 130 feet of which occur before the
brow of the steep part of the hill is reached. The fauna is as follows:

176 Report oF THE STareE GEOLOGIS?.

Chonetes scitula, Hall. (c)
2. Chonetes setigera, Hall. (c) -
3. Phynchonella (Camarotech ia) eximia, Hall.
4. Spirifer mucronatus (Con.), Bill. (1)
5. Tropidoleptus carinatus (Con.), Hall.
6. Paracyclas lirata (Con.), Hall. (11)
7. Nucula corbuliformis, Hall. (ar)
8. Modiomorpha subalata (Con.), H., var. Chemungensis, H. (rr)
9, Actinopteria ct. Theta, Hall. (ar)

Morris.

Morris township, Otsego county, les on the eastern side of the Unadilla
river, directly east of the southern part of New Berlin township.

XX J", The hill on the eastern side of the river is steeper than the
one on the western side, but unfortunately does not afford frequent exposures
of the rocks. The road crossing the river south of schoolhouse No. 4 and
section C, continues almost due south for over one mile until it reaches the
east and west road on top of the divide. There are but few exposures along
the steep road, most of the rocks being concealed by drift. At 305 feet above
the river are rather thin sandstones, and loose pieces from apparently near
this horizon contain some fossils. The species below were obtained from
the loose blocks:

1. Orthothetes Chemungensis (Con.), Hall. (a)

Abundant in the few blocks of stone found at this place.

2. Phacops rana (Green), Hall. (1r)

3. Modiomorpha subalata (Con.), Hall, var. Chemungensis, H. (vr)

4. Actinopteria, sp. (1r)

The greater part of the hill probably belongs in the Ithaca formation,
with a hundred feet or so of the Sherburne formation at its base.

XX P*. On the east and west road of the divide just east of the
corners in the western part of Morris township are red, thin-bedded sand-
stones which alternate with those that are thin, green and coarse-grained.
This outcrop is apparently near the base of the Oneonta formation. In the

field to the north of the nghway, some ten feet higher, is a ledge of grey,

ProssER—HaminroN and CremunG SeErtes. ep

thin-bedded, coarse-grained sandstones, above which are red sandstones of
similar texture. This is a characteristic outcrop of the Oneonta sandstone.

The accompanying sketch gives an idea of the divisions of section D.

SECTION OF XX D, SOUTH OF NEW BERLIN CENTER.

(Sy Nee Heavy ledge of red and grey sandstone.
Oneonta.
|
~— | . .
655! |e Red and greenish thin sandstones.

ios Tthaca.
BOB! pe D'. Sandstones.
305’ | Covered. Sherburne.

ian.) Unadilla river level.

On the “Preliminary Geologic Map of New York,” published in 1896,
the northern point of the Oneonta sandstone is represented as some two
miles farther south; but the formation clearly forms the summit of the
divide in this locality.

Two miles to the east 1s another four comers, where the road crosses the
valley of Morris creek in the northern part of Morris. Near the corners,
approximately 220 feet lower than the ledge of Oneonta sandstone at D®, are
thin arenaceous shales which contain the small form of Sp/r/fer mucronatus
(Con.), Bill. These rocks belong in the Ithaca formation, which continues
northward and encloses the small glacial lake on the line of Morris and
Pittsfield townships well toward the summit of the divide known as
Matteson’s lake.

XX /. At the top of the hill, northwest of Matteson’s lake and over-
looking the Unadilla valley, are thin arenaceous Ithaca shales, this formation
continuing for at least 350 feet below the summit of the hill. An outcrop of
these shales about fifty feet below the summit contains plenty of Ithaca fossils.
The lower part of the hill belongs in the Sherburne formation which extends
along the river road to north of the four corners above Silver lake.

We,

178 Report or THE SratreE GEOLOGIST.

Pittsfield.

Pittsfield township, Otsego county, is on the eastern side of the Unadilla
river and lies east of the northern part of New Berlin and the southeastern
corner of Columbus.

The line of division between the Hamilton and Sherburne formations
runs in a northeasterly direction along the side of the hill east of the Unadilla
river and Wharton creek to about two miles northeast of Pittsfield village,
when it takes a more easterly course across the divide between Wharton and
Butternut creeks. This line is twelve miles due north of that represented
as the top of the Hamilton formation on the “Preliminary Geologic Map
of New York”; but this difference, which will be found across Otsego
county and still farther eastward, is due to the fact that the Sherburne and
Ithaca formations were mapped as the upper part of the Hamilton in eastern
New York.

Fossiliferous Hamilton shales and sandstones on the eastern bank of the
Unadilla river in the northwestern part of Pittsfield, as well as the barren
Sherburne shales and sandstones forming the long Pittsfield hill southeast of
New Berlin, crossed by the New Berlin and Morris road, the top of which is
capped by the Ithaca formation, were described by the writer several years
ago.’

The lower part of the hill east of Wharton creek and New Berlin village
shows ledges of arenaceous shales and thin sandstones which contam plenty
of characteristic Hamilton fossils. Above, and approximately 135 feet higher
than the railroad crossmg below New Berlin, are thin, blue, unfossiliferous
sandstones and shales that belong in the Sherburne formation. This indicates
that the base of the Sherburne occurs at about the same elevation east of the
Unadilla river as in West creek in New Berlin village.

XX /". On the hillside east of Wharton creek, one-fourth mile north-
east of Pittsfield village and about 180 feet above the railroad level of New
Berlin, are rough arenaceous shales containing numerous Hamilton fossils.
Ten feet higher are thin unfossiliferous sandstones which are perhaps in the

base of the Sherburne. The fauna of F! is as follows:

1. Spirifer granulosus (Con.), Hall. (a)
2. Tropidoleptus carinatus (Con.), Hall. (aa)
3. Cyrtina Hamiltonensis, Hall. (ar)
4. Ambocelia umbonata (Con.), Hall. (1)

1 Twelfth Annual Report State Geologist [New York], pp. 133-136,

PRossER—HAMILTON AND CHEMUNG SERIES. 179

5. Modiomorpha concentrica (Con.), Hall. (rr)
6. Paleoneilo emarginata (Con.), Hall. (17)
7. Mytilarca (Plethomytilus) oviformis (Con.), Hall. (r)
8. Crinoid segments and part of stems. (c)

XX F?. On top of the hill, one and one-half miles northeast of Pitts-
field and near the township line between Pittsfield and Edmeston, are thin,
rather irregular arenaceous shales containing Hamilton fossils. The top of
the hill is barometrically 370 feet above the railroad at New Berlin, but it is
two and one-half miles: northeast of the locality at which the top of the
Hamilton was found at an altitude of 135 feet above the railroad, and if the
dip remains seventy feet or more per mile it would bring the top of the
Hamilton near the summit of this hill. The nature of the rocks and fauna
seems to favor the above conclusion and shows that the entire hill is com-
posed of Hamilton rocks. Eighty feet below its summit are very coarse
shales grading into sandstones that form rather prominent ledges containing
an abundance of Hamilton fossils. Sperifer granulosus (Con.), Hall, is abun-
dant; Zropidoleptus carinatus (Con.), Hall, common; Pleurotomaria capil-
lavia, Con., rare. A careful search would yield considerable numbers of
characteristic Hamilton species.

.For some distance along the first brook entering Wharton creek from the
east, one and one-half miles above Pittsfield, the fossiliferous Hamilton shales
are found. To the south on the hillside the shales and sandstones of the
Sherburne occur, while on the igh hill to the south, 500 feet above the
Hamilton shales in the brook, are those containing the fossils of the Ithaca
formation. This exposure occurs on the high hill to the north of Ketchum.
However, on account of the thick deposit of drift covering the rocks of the
divide between the Wharton and Butternut creeks, it is difficult to describe

very closely the geological formations of the region.

GEOLOGY OF SouTHERN OtTsEGoO CounrTy.

The southern part of Otsego county is covered by rocks belonging to the
Hamilton, Sherburne, Ithaca and Oneonta formations. In tracing the line of
division between the Hamilton and Sherburne formations across this county,
the geology of its southern part was quite carefully studied and will now be
described.

180 Report oF tHe State GEOLOGIST.

New lisbon!

NX fH?. In the northwestern part of the township, one and one-half
miles northwest of Garrattsville, is a small glacial lake known as Turtle lake.
The ground is marshy about the lake, but along its outlet and in a small run
which enters the brook from the south are rocky ledges. The arenaceous
shales on the outlet of Turtle lake are apparently im the Hamilton formation,

fossils bemg common, as the following list will show :

1. Lropidoleptus carinatus (Con.), Hall. (a)
2. Spirifer mucronatus (Con.), Bill. (rr)
3. Spirifer granulosus (Con.), Hall. (1r
4. Sporifer Tullius, Hall. (ar
5. Cyrtina Hamiltonensis, Hall. (1r)
6. Microdon (Cypricardella) tenwistriatus, Hall. ar
7. Microdon (Cypricardela) bellistriatus, Hall. (rr)

It is somewhat difficult to determine sharply the line between the Hamil-
ton and Sherburne on this hill, Shales or thin sandstones containing but a
few fossils continue for forty feet up the small run southwest of the main
creek. A few of the Hamilton species in this locality seem to occur somewhat
above the horizon of the top of the Hamilton, in shales which, farther west,

are in the lower part of the Sherburne.

NX H'. Sixty-five feet above the outlet of Turtle lake, greenish shales
and sandstones begin and continue for fifty feet to the top of the hill. These
rocks contain a few fossils; thirteen specimens of Liorhynchus mesacostalis,
Hall, and two of Spirifer mucronatus (Con.), Bill., were collected beside speci-
mens having fucoidal markings. These fifty or more feet of shales and sand-
stones are regarded as belonging in the Sherburne formation, but it appears
that the unfossiliferous fine blue shales of the Unadilla valley have changed
into these more arenaceous shales in which Leorhynchus is not uncommon.
In the brook to the west of Turtle lake and near the divide, are smooth rocks
which may belong in the Hamilton, while the loose ones on the ground are
very similar to the Sherburne. The elevation of this locality is about the
same as the horizon considered as the top of the Hamilton south of Turtle
lake, but on account of the heavy deposit of drift over the region of the
divide, it is difficult to determine accurately the underlying geologic for-
mation.

XX HH. Ledges near the upper part of the glen, one-half mile north-

west of Garrattsville and 120 feet higher than the village hotel. ‘The rocks

ProssEr—Haminton AND Curmune SrErIes. 18]

consist of shales and thin sandstones and contain plenty of Hamilton

fossils. Typical Hamilton rocks with the characteristic fauna of the for.

mation,
1. Tropidoleptus carinatus (Con.), Hall. (c)
2. Spirifer mucronatus (Con.), Bull. (1)
3. Spirifer Tullius, Hall. (c)
4. Cryptonella (.Yunella) Linckleni, Hall. (a)
5. Stropheodonta perplana (Con.), Hall. (ar)
6. Palwoneilo fecunda, Hall. (ar)
7. Paleoneilo constricta (Con.), Hall. (rr)
8. Schizodus appressus (Con.), Hall. (rr)
9. Leda diversa, Hall. ar)
10. Grammysia cuneata, Hall. (rr)
11. Grammysia arcuata (Con.), Hall. (rr)

XX //'. In this same brook at the foot of the glen and only fifteen feet
above the hotel, are argillaceous, blue, soft Hamilton shales, contaiming an
abundant Hamilton fauna. The dip is heavy to the southwest, judging from
the exposure in the brook. The following species were collected in a short

time:

1. Tropidoleptus carinatus (Con.), Hall. (a)
2. Spirifer mucronatus (Con.), Bill. (c)
3. Spiriter Tullius, Hall. (rr)
4. Grammysia alveata (Con.), Hall (?). (1r)
5. Nuculites triqueter, Con. (c)
6. Lunulicardium fragile, Hall (2). (rr)

Rather heavy concentric undulations like Puracyclas; too
imperfectly preserved for positive identification.
Chonetes lepida, Hall (?). (ar)

Specimens do not show the stronger striae near the center,

~T

although one is apparently the ventral valve.

8. Pleurotomaria capillaria, Con. (2). (1r)
9. Pholadella radiata (Con.), Hall. (ar)
10. Phacops rana (Green), Hall. (rr)
11. Aviculopecten, sp. (rr)

A section partly along this brook from Garrattsville northwest to Turtle

lake is as follows:

182 Report oF THE Stare Groocist,

BAI! |
\ |
50’ | Ht Sherburne.
275!
25’ | Covered. Hamilton.
ya Oe | ace
ie AOY os
OW Oe ales | H®. Outlet of Turtle lake.
90’ | Partly covered.
P20 Wee ees
| 105’ | Glen. Hamilton.
1!) oe eee
|
15’ | Covered.
0’ |---| Garrattsville hotel level.

The hill on the western side of Butternut creek below Garrattsville is
steep, but pretty well covered with drift, so that exposures of rocks are some-
what infrequent. About one and one-half miles below Garrattsville, Hamilton
shales show by the roadside, while in the field, 150 feet higher, are rather
thin arenaceous shales which run into sandstones and contain but few fossils,
apparently in the upper part of the Hamilton. Seventy-five feet higher, or
225 feet above the road, are thin sandstones apparently in the Sherburne for-
mation. Along the valley, three and one-quarter miles below Garrattsville and
a short distance above Stetsonville, are rocks belonging in the Hamilton
formation. On the road west, one hundred feet above the valley, are
smooth, arenaceous, thin sandstones of the Sherburne formation. ‘This
agrees with the exposures of Sherburne found to the northwest in Pitts-
field township about Ketchum, where the valleys and lower hills are
composed of the Sherburne, with the Ithaca forming the summits of the
higher hills.

The Hamilton probably follows the creek valley for a mile or more below
Stetsonville, before reaching its upper limit. A dip of seventy feet per mile

to the south would just about brig down what was called the top of

ProsseER—Haminron AnD CrEemuncG SrErIes. 183

the Hamilton on the hill south of Turtle lake to the level of the high-
way at Stetsonville. On the hillside, one mile below Stetsonville, and
three miles northeast of Morris, are even-bedded, thin sandstones and

arenaceous shales, in which no fossils were found belonging to the Sherburne

o
formation.

One hundred feet higher, or 210 feet above the highway are shaly,
arenaceous rocks (XX G*) that contain abundant specimens of Atrypa retic-
ularis (Linné), Dal., and a few other fossils. This ledge is probably in the
lower part of the Ithaca formation. Below are more even-layered shales, with
an occasional fossil similar to those in the more arenaceous portions of the

Sherburne. The fauna of G' is:

1. Atrypa reticularis (Linné), Dal. (a)
Rather small and gibbous specimens.

2. Chonetes, sp. (rr)

3. Lchinocaris cf. punctata, (Hall), Whitfield. (11)

Part of the impression of the cephalothorax whose surface

markings resemble those of this species.

XXT 4. Kast of the Butternut Creek, and directly east of Noblesville,
near the foot of the hill, are quite smooth, greenish sandstones, in the midst
of which are blocky shales in which Pehynchonella venustula, Hall, is common.
A few other species are associated with the Rhynchonella, but they occur
sparingly. Below this horizon are bluish shales which were shown in an
excavation for a well, while higher on the hillside, along a small run, are thin,
arenaceous shales, evidently the Sherburne formation, in which fossils were
not found. The fauna of B! is:

1. Spirifer mucronatus (Con.), Bill. (rr)

2. Atrypa reticularis (Linné.), Dal. (1)
The rather small form.

3. Lropidoleptus carinatus (Con.), Hall. (rr)

4. Rhynchonella (Lypothyris) venustula, Wall. (c)

While engaged in the field work necessary for determing the top of the
Hamilton formation in the Butternut valley, the line of separation between
the Hamilton and Sherburne formations was indicated as approximately the
same horizon as that at which Rhynchonella venustula was found. Later,
the specimens were carefully compared with the figures of this species and

authentic specimens from the State Museum, and it was found that in form,

184 Report or tHe Srare Groroatst.

number of pleations in fold and sinus, and im vascular markings the speci-
mens from Noblesville agree closely with typical specimens of /thynchonella

venustula.

KkWYNCHONELLA (HYPOTHYRIS) VENUSTULA, Hall.
Noblesville, N. Y.

1. Partially exfoliated pedicle-valve, showing seven plications in the sinus.
2. Internal cast of pedicle-valve, showing vascular markings.
3-5. Front, lateral and cardinal views, showing the strongly gibbous form of the specimens.

The distribution of Lhynchonella venustula, Hall, which is either iden-
tical with or very closely related to the European species 72. cuboides, Sowerby,
has previously been confined to a belt of country in central New York,
extending from Madison county on the east to Yates county on the west, and
in its range Professor Hall reported the species “in the Tully limestone, at
Tully and Tinker’s falls in Onondaga county ; at Ovid in Seneca county ; at
Benton and Penn Yan in Yates county, New York.”! The final volume of
the Palaeontology of New York (Brachiopoda IIT) does not indicate either a
greater distribution or range for the New York species, although it notes its
close relationship to the 72. cuboides of Europe. The species has also been
considered by Professor H. 8. Willams in a paper on “The Cuboides Zone
and its Fauna,” but no mention is made of its occurrence at additional
localities.? Professor 8. G. Wilhams in his paper on “The Tully limestone,
its Distribution and its known Fossils,” reported. the species from South
Lebanon in the southern part of Madison county,* which, as far as the writer
is aware, was its farthest known eastern distribution previous to its discovery
in Otsego county.

! Geological Survey, New York, Palaeontology, Vol. TV., Part I., 1867, p. 348.
2 Thid., Vol. ViIL, Part I1., 1894, p. 200.

4 Bulletin Geological Society of America, Vol. I., pp. 481-500.

4 Sixth Annual Report State Geologist [New York] 1888, pp. 18, 27.

Haminton AND CremuNnG SeErres. 185

Prosser

The discovery of /?. venustu/a at Noblesville extends its distribution
thirty miles farther to the southeast than heretofore reported ; and on account
of the very limited known range of the species this discovery is regarded as
very strong evidence in support of the horizon considered in this report as the
top of the Hamilton formation. The species was also noted at this position
in the geological series at a few other places in Otsego county, and so it seems
to the writer that this question as to where the line of division between the
Hamilton and overlying formation is to be drawn in that county, should be
finally settled by this evidence. This seems a perfectly tenable position,
especially since the closely related species, /?. venustula, of New York, and
LF. cuboides, of Europe, are regarded as occurring at very nearly the same
geologic horizon. In the words of Professor H. 8. Willams: “The correlation
thus established is one not merely of homotaxy, but within relatively short
limits, of contemporaneity ; and that the Tully lmestone may be said to have
been deposited during the period of deposition of the Cuboides Schichten, of
England, Belgium, France, Germany, Russia and the East.”

Along the road and a small stream to the southeast of Noblesville, are
occasional exposures of smooth, unfossiliferous shales and thin sandstones
belonging in the Sherburne formation.

XAT L*. At the summit of the hill, 360 feet by the barometer above
the ledge with Rhynchonella venustula, are quite fossiliferous, arenaceous

shales and thin sandstones affording the following species :

1. Spirifer mesastrialis, Hall. (c)
2. Spirifer mucronatus (Con.), Bill. (rr)

3. Lthynchonella (Camarotechia) eximia, Hall (¢).
Rather small specimens with sharp plications.

The specimens of Spirifer mesastrialis are typical and common, indicating
these rocks to be in the Ithaca formation. It is probable that the base of the
Ithaca beds is a hundred feet lower than the summit of the hill, and that the
high land between Noblesville and Gilbert’s lake belongs in this formation.

XXY7 OC". At the three corners on the road following the township line
between New Lisbon and Laurens, one-third of a mile west of Gilbert’s lake,
are rather coarse shales that are very fossiliferous, especially thin layers which
are largely composed of Spirifer mesastrialis, Hall. A very brief time was
spent in collecting, and only two other species were noted, viz.: Atrypa
reticularis, (Linné), Dal., and Tropidoleptus carinatus (Con.), Hall. This

locality is, according to one barometric reading, seventy feet lower than

1 Bulletin Geological Society of America, Vol. I., p. 498.

186 Report oF THE STATE GEOLOGIST.

XXI_ B? at the summit of the hill southeast of Noblesville, and 510 feet above
the hotel in Laurens, four miles to the southeast im the valley of Otego creek.

To the north of Noblesville are occasional exposures of rather coarse,
arenaceous shales in which Hamilton fossils are not uncommon. <Afrypa
reticularis (Linné), Dal., is one of the most common species. The shales
with this species are exposed near the three corners, one and one-half miles
northeast of Noblesville (XXIV D*), and still better shown in the ledges
along the hillside in the northern part of school district No. 8. In the coarse
arenaceous shales of XXIV D* there was little opportunity for collecting,

and only the three following species were noted :

1. Atrypa reticularis (Linné), Dal. (c)
2. Productella, sp. (1)

A large species similar to the one found at XXIV D+ N. E. of
Gilbert’s lake.

3. Phacops rana (Green), Hall.

Hamilton ledges with characteristic fossils are well shown on the steep
hillside above the corners, about one and one-quarter miles south of Garratts-
ville. To the northeast of the locality just mentioned and east of Garratts-
ville is a steep hill, the top of which may be capped by rocks belonging to the
Sherburne formation. By the highway on the eastern side of the hill and
about north of New Lisbon Centre are coarse, arenaceous Hamilton shales,
which show glacial striae running 8. 50° W.

Near the top of the hill to the northeast a loose piece of stone was found
in the field in which Rhynchonella (Hypothyris) venustula, Hall, is common.
In the same block was an internal impression of Spirifer mucronatus (Con.),
Bill., and a Chonetes, sp. This block probably came from the same horizon
as the one east of Noblesville in which the /ehynchonellas were found in place,
and this indicates the extension of that horizon to the northeastward on the
high hill in the northern part of New Lisbon. The top of the hill is so
thoroughly covered by drift that exposures of the bed rock are rare; but the
larger part of the loose pieces are apparently from the Hamilton formation
mixed with unfossiliferous pieces, possibly from the Sherburne beds.

NNT A’. To the northeast of Garrattsville a road climbs the steep hill
east of Butternut creek, the summit of which is two miles from the village,
giving a section of nearly 500 feet of Hamilton rocks. About one and one-
half miles N. EK. of Garrattsville and 335 feet above the level of Butternut
creek are conspicuous ledges of bluish and iron-staimed blocky shales that con-

tain plenty of characteristic Hamilton fossils. One hundred and twenty feet

Pross—ER—HaAmintron and CHEMUNG SrErIEs. 187

higher, on the road near the top of the hill are bluish shales (X XI A’), con-
taining numerous fossils belonging in the Hamilton formation. In a few
minutes, specimens of the following species were found :

1. Spirifer mucronatus (Con.), Bill. (c)
2. Cyrtina Hamiltonensis, Hall. (1r)
3. Ambocelia wmbonata (Con.), Hall. (11)

About thirty-five feet higher on the road running southwest, shales and
thin sandstones outcrop which contain Hamilton fossils. This seems to show
that the summit of the high hill two miles northeast of Garrattsville is in
the Hamilton formation.

The section may be tabulated as follows:

SECTION OF HIGH HILL NORTHEAST OF GARRATTSVILLE.

AOQe jaa es Shales at top of hill, Hamilton.
35°
a = A*. Bluish shales with Spirifer mucronatus.
120% 4
BO ee: 0s A’, Blocky shales.
335/
(\) | anaes | Level of Butternut creek, Hamilton.

XXIV D*. Exposures of rather coarse, bluish shales at the lower end
of the gorge one mile northeast of Noblesville and in the first brook north of
that village. In these shales specimens of Liorhynchus are common, which
are probably ZL. mesacostalis, Hall, although there is a decided tendency in
the striae to remain on the sides of the shells as is the case with Z. mu/ticosta,
Hall. It is probable that these shales are in the Sherburne formation,
although they may perhaps represent the extreme upper part of the Hamilton.
Twenty feet higher is an excellent outcrop of bluish, argillaceous shales in
which no fossils were found.

XXIV DP’. At the head of the gorge, two miles northeast of Nobles-
ville, are bluish and olive argillaceous shales, with an oceasional thick stratum
of sandstone; these, according to the barometer, are 195 feet higher than D*.
In some of these shales specimens of Productel/a are abundant, and the fauna _
would indicate the lower part of the Ithaca formation. Judging from several
observations in the southern part of New Lisbon, the dip is very heavy to the

southwest. The fauna of D®° is:

188 Report oF THE STatE GEOLOGIST.

1. Productella, sp. | (a)
Apparently between P. speciosa, Hall, and P. lachrymosa
(Con.), Hall. One of the specimens is truncated at the beak.
2. Atrypa reticularis (Linné), Dal. (rr)
3. Palwoneilo constricta (Con.), Hall. (11)
Almost identical with the small one figured on plate 48, figure
16 (Palaeontology of New York, Vol. V, Part I), from Ithaca,
INS
4. Coral, sp. (rr)
5. Actinopteria eta, Hall (?). (1r)

XXIV 4. Ledges of coarse, arenaceous shales on the hillside west of
Pool creek, three and one-third miles east of Noblesville and about three-
quarters of a mile northeast of Gilbert’s lake. The shales merge into thin
sandstones which, on the weathered surfaces, are brownish from iron stain.
The ledges show a heavy dip to the southwest. According to the barometer,
this locality is 125 feet higher than D®*, and 320 feet above D®. In these shales

specimens of Atrypa and Productella are common, the complete fauna being:

1. Atrypa reticularis (Linné), Dal. (c)
2, Productella, sp. (c)
The specimens are large, with wrinkles and folds on the ears.
3. Chonetes setigera, Hall. (rr)
4. Grammysia subarcuata, Hall (¢). (ir)

From a hasty examination of this region I was not able to positively
determine the formation, and it is quite possible that on the accompanying
geologic map the top of the Hamilton is represented somewhat too far to
the south in the valley of Pool creek.

XXIV J. On the divide between Pool creek and Fall brook, one and
one-half miles east of D‘, are thin bluish and olive shales in which no fossils
were found. This locality is in the southeastern part of New Lisbon, school
district No. 16, and is, according to the barometer, 470 feet above the level of
Otego creek at Mt. Vision, two and one-half miles to the southeast.

XXIV /*. On the eastern side of the hill, by the roadside, about 110
feet below D**, are rather argillaceous shales in which Hamilton fossils are
common, especially typical specimens of Spirifer mucronatus (Con.), Bill.
These shales are clearly in the Hamilton formation, the top of which is then
fully 360 feet above the level of Otego creek at this place. The fossils are:

1. Spirifer mucronatus (Con.), Bill. (a)

9. Ambocalia wumbonata (Con.), Hall. (c)

ProssER—HAMILTON AND CHEMUNG SERIES. 189

3. Stropheodonta perplana (Con.), Hall. (rr)
4. Atrypa reticularis (Linné), Dal. (11)
5. Palwoneilo emarginata (Con.), Hall. (rr)

XXIV I”. Somewhat below the above locality the rocks of the hillside
are well exposed along the gorge of Fall brook, which has rocky banks with
the

gorge are clearly Hamilton in age. In the upper part of the gorge above the

several cascades in the course of its steep descent. All the rocks along
upper bridge are bluish, arenaceous shales. Those near the top are thinner,
and the layers more even, approaching thin sandstones in texture. The upper
shales of the brook are about 230 feet above the level of the Otego creek, at
Mt. Vision, one and three-quarter miles to the southeast. Fossils are com-
mon, and careful collecting would yield a fairly large number of species. The

following were obtained in a short time:

1. Spirifer granulosus (Con.), Hall. (7)
2. Terebratula (Hunella) Lincklaeni, Hall, (rr)
3. Ambocelia wmbonata (Con.), Hall. (1)
4. Spirifer Tullius, Hall. (c)

One of the noticeable features in the palaeontology of Otsego
county is the large number of specimens of the above species in

the upper Hamilton.

5. Spirifer fimbriatus (Con.), Bill. (1r)
6. Tropidoleptus carinatus (Con.), Hall. (ir)
7. Stropheodonta perplana (Con.), Hall (2). (17)
8. Chonetes setigera, Hall. ar)
9. Nucula bellistriata (Con.), Hall. (1)
10. Palwonetlo perplana, Hall. (rT)
11. Grammysia (Sphenomya) cuneata, Hall. (c)
12. Phacops rana (Green), Hall. (rr)

Under the upper bridge of Fall brook is a stratum containing numerous
specimens of Spirifer granulosus (Con.), Hall.

AXIV DP. At the foot of the gorge, only sixty-five feet above the
Otego creek, are bluish, rather coarse, arenaceous shales which contain plenty
of fossils, especially Zropidoleptus carinatus (Con.), Hall. The list is as
follows:

1. Tropidoleptus carinatus (Con.), Hall. (a)
2. Spirifer mucronatus (Con.), Bull. (1)
3. Spirifer granulosus (Con.), Hall. (rr)

4. Microdon (Cypricardella) tenuistriatus, Hall. (rr)

190 Report OF THE STaTE GEOLOGIST.

The following diagram will give an idea of the Fall brook section,
extending from one and one-half to two and one-half miles northwest of Mt.

Vision:

ATO) eae D**,. On divide, blue shales of Sherburne.
110°
360) D®. On road, Spiriter mucronatus, Hamilton.
130/
230’ |-———-| D*. Near top of rocks in Fall brook.
100
130°... Abundant specimens of Spirifer granulosus.
69/
65" |= D'. Foot of Fall brook gorge. Hamilton.
65’ = Covered.
O! Sis Level of Otego creek at Mt. Vision.
Laurens.

The township of Laurens lies directly south of New Lisbon, except the
northeastern corner, which is south of Hartwick, the township adjoinmg New
Lisbon on the east. Otego creek flows through the eastern part of the town-
ship, bordered by a very steep hill on the eastern side, broken only by small
brooks, the largest being Keyes brook in the northeastern corner of the town-
ship. The ridge on the western side of Otego creek is not nearly as steep
as the one on the eastern side, and it is broken by a number of brooks and
creeks of fair size, with corresponding valleys.

XXIV (. Shghtly northeast of the village of Mt. Vision, in the north-
eastern corner of the township, is a steep hill, which rises 375 feet above the
Otego creek, known as Mt. Vision. The hill hes between the valleys of
Otego creek and Keyes brook, the latter being at its greatest distance only a
little more than one and one-half miles east of Otego creek. The hill has, of
course, been formed by the erosion of the streams on its eastern and western
sides, with its steeper flank toward the larger stream and tapering to a point
opposite the junction of the two streams. On the hillside, one hundred feet

above the creek, are prominent ledges of coarse, arenaceous shales. They are

ProsseEr—Haminttron AND CHEMUNG SeErRIEs. 191

quite coarse-grained, with every lithologic appearance of the coarser Hamil.
ton, while the abundant Hamilton fauna refers them unquestionably to that
formation. The list is:

1. Spirifer. Tullius, Hall. (c)
2. Spirifer mucronatus (Con.), Bill. (c)
3. Spirifer granulosus (Con.), Hall (4). (rr)
4. Tropidoleptus carinatus (Con.), Hall. (c)
5. Chonetes coronata (Con.), Hall. (rr)
6. Ambocelia umbonata (Con.), Hall. (ar)
7. Stropheodonta demissa (Con.), Hall. (1)

8. Microdon (Cypricardella) tenuistriatus, Wall (4). (ar)
Probably young specimens of this species, though they resemble

somewhat figures 19 and 20, plate 73 of J. bel/istriatus, Con.

9. Téellinopsis subemarginata (Con.), Hall. (11)
10. Modiomorpha mytiloides (Con.), Hall. (1r)
11. Glyptodesma erectum (Con.), Hall. (rr)
12. Pterinea flabella (Con.), Hall. (ar)
13. Liopteria DeKay?, Hall. ar)
14. (4) Psilophyton princeps, Dn. (rr)

Fragment.

Near the top of the hill, about 207 feet above the base of C', is
an irregular, concretionary stratum, similar to those which are not

unfrequently found in the upper Hamilton and higher formations of eastern

New York.

XXIV C*. At the top of the steep escarpment, near the brow of the
hill, some 350 feet above the creek level, are thin sandstones and _ shales,
certain layers of which contain many specimens of Spirifer mucronatus (Con.),

Bill. The following species were collected :

1. Spirifer mucronatus (Con.), Bill. (a)
2. Cyrtina Hamiltonensis, Wall. (rr)
3. Orthothetes Chemungensis (Con.), Hall. (rr)
4. Ambocelia umbonata (Con.), Hall. (rr)
5. (4) Aviculopecten princeps (Con.), Hall. (ar)

The rocks and fauna of this outcrop are similar to those of XXIV D*, on
the western side of Otego creek, about 360 feet above its level. It seems
clear that the Hamilton formation extends to the top of the ledges on

Mt. Vision and forms nearly, if not quite all of the hill.

192 Report oF THE Srare GEOLOGIST.

SECTION OF MT. VISION.

One
Top of Mt. Vision.
350’ C*. Hamilton ledges at brow of hill.
43/
SO ae ee | Concretionary stratum,
207
100° |---| (Oi Hamilion:
L100’
Oe al Level of Otego creek at Mt. Vision.

AXIV B*. About three-quarters of a mile south of Mt. Vision, on the
eastern side of Otego creek, is a rocky hillside on the Field farm, known
locally as the “Owl Patch.” A short distance farther south, the point of the
nll strikes the highway about seventy-five feet above the creek level, and
thin, argillaceous, quite fossiliferous shales of bluish or olive color with thin
strata of sandstone are quite well exposed by the roadside. The following

species were obtained :

ll. Spiriter INUCPONAELUS (Con.), leadlil. (c)
2. Atrypa reticularis (Linné), Dal. (11)
3. Gontophora Hamiltonensis (Hall), Miller. (11r)
4. Nuculites oblongatus, Con. (1r)

d. Platyceras, sp.

XXIV L*. Seventy-five feet higher on the hillside, in the “Owl Patch,”
are conspicuous ledges of coarse, arenaceous shales, in lithologic character and
fauna similar to those of the lower ledges (XXIV C') of Mt. Vision. This
outcrop belongs in the Hamilton formation, and the fossils are abundant and

typical, as will be seen below :

1. Spiriter mucronatus (Con.), Bull. (c)
2. Tropidoleptus carinatus (Con.), Hall. (1")
3. Spiriter Tullius, Hall. (c)
4, Tellinopsis subemargtinata (Con.), Hall. (11)
5. Microdon (Cypricardclla) tenuistriatus, Hall. (a)

These specimens are smaller than the figures of this species and
perhaps are the forms of I. be//istriatus, Con., which have fine
striae, but they agree with the description of the young forms of
M. tennistriatus, Hall.

6. Nucula corbuliformis, Hall. (11)

Grammysia arcuata (Con.), Hall. (ar)

~J;

ProssER—HAMILTON AND CHEMUNG SERIES. 193

8. Palwoneilo constricta (Con.), Hall. ar)
9. Liopteria DeKayi, Hall (2) (c)
All imperfectly preserved.

NNXIV 5°. Ledges are rather conspicuous on the hillside towards its
top, and 170 feet above B? is a prominent ledge of even-bedded, thin sand-
stones forming the upper terrace of the hillside. These sandstones are fine-
grained, greyish to slightly olive in color, weathering to a brownish grey.
Portions of them are literally filled with specimens of all sizes of /e?hynchonella
venustula, Hall, although scarcely any other fossils occur; a broken specimen
Paracyclas lirata (Con.), Hall (2), being the only one noted. In the loose
fragments among the talus, apparently from this ledge, were pieces of rock
containing abundant specimens of Spirifer mucronatus (Con.), Bill., and a
single broken specimen of Palwonetlo emarginata (Con.), Hall (2). The hill
is rounded above this ledge and does not extend much higher, and the rocks
are covered by soil; but the presence of the abundant specimens of /?/yn-
chonella venustula indicates that the Hamilton formation extends nearly to its
summit. This ledge is 320 feet above the level of Otego creek, and when the
hill is compared with Mt. Vision, rather more than three-quarters of a mile to
the north, the highest rocks of which are 350 feet above the creek level, or
the top of the hill approximately 3875 feet above the creek, it will be seen
that all of that bill must belong in the Hamilton formation, since a dip of
seventy-five feet per mile, probably less than the true dip, would carry the
Hamilton rocks over the summit of Mt. Vision.

This Pehynchonella venustula ledge is seven miles southeast of the locality
already described near Noblesville, carrying the distribution of the species so
much farther eastward, as well as fixing precisely in the Otego valley a point

for the separation of the Hamilton and Sherburne formations.

SECTION OF THE “ OWL PATCH,” THREE-QUARTERS OF A MILE SOUTIL OF MT. VISION.

B20pye B®, Thin sandstones with abundant specimens of
ry. ‘ L
Phynchonella venustula, Top of Hamilton.
Oy
150! | --= B?. Coarse, arenaceous shales, abundant Hamilton
1D | fossils,
TB |e BB. Hamilton shales on highway.
ay as
Of fen Otego creek level.

194 Report oF THE Strate GEOLOGIST.

AXAXTV A‘. Shales and thin blue sandstones by the side of the highway
along Lake brook, one-half mile northwest of Laurens. This locality is about
three miles southwest of the “Owl Patch” (XXIV B?&*), and 110 feet above
the main street of Laurens. In some layers there are plenty of fossils,

especially Spiriter mucronatus (Con.), Bill. ‘The complete list is as follows :

1. Spirifer mucronatus (Con.), aN (a)
2. Tropidoleptus carinatus (Con.), Hall. (ar)
3. Atrypa reticularis (Linné), Dal.

4. Conularia undulata, Con. (rr)
5. Athyris Cora, Hall (?). (17r)

NXIV <A*. Coarse, arenaceous shales on hill, one and four-tenths miles
northwest of Laurens and 260 feet above the main street. They form a
prominent outcrop in the field on the eastern side of the east and west cross-

road, and contain numerous specimens of Atrypa reticularis and Spirophyton.

The list is:

1. Atrypa reticularis (inné), Dal. (a)
2. Cyrtina Hamiltonensis, Hall. (ar)
3. Productella, sp. (c)
4. Actinopteria decussata, Hall (2). (17)
5. Spirophyton, sp. (rr)

These shales of XXIV A‘ and A?, resemble those of the Hamilton group
more than they do those of the Ithaca formation.

Hartwick.

Hartwick township lies east of New Lisbon and Burlington, and north
of Laurens and Milford townships, its southern half extending eastward to
the Susquehanna river. The topography of the southern half exhibits steep
hills bordering narrow valleys, the most important of which is the Sus-
quehanna.

XXIV ©. Inthe southern part of the township, two and one-half
miles northeast of the village of Mt. Vision, is a high hill, known as Bowie
hill, the summit of which is approximately 750 feet higher than the valley
of Otego creek at Mt. Vision. Above the top of Mt. Vision which, as already
stated, is in the Hamilton, the rocks are mostly covered by drift. At the
school-house No. 15, on the road directly south of Bowie hill, are bluish,
argillaceous shales, very similar to the Sherburne formation, in which only a

single specimen of Chonetes setigera, Hall, was found.

ProssER—Hamitten and CHEMUNG Serres. 195

XXIV C4, Near the summit of Bowie hill, some 715 feet above Otego
creek, about one-half mile southwest of Arnold lake, is an outcrop of rather
coarse-grained, bluish to dark grey sandstone, containing numerous specimens
of Spirifer mesastrialis, Hall. There are shaly partings with iron concretions,
and these shales are more fossiliferous than the massive sandstones, for they
contain numerous specimens of Spirifer mucronatus (Con.), Bill.; 7 roptdolep-
tus carinatus (Con.), Hall; Chonetes setigera, Hall; Phynchonella Stevensi,
Hall, and Liorhynchus mesacostalis, Hall. Loose pieces of bluish, arenaceous
shales scattered over the top of the hill contain specimens of Liorhynchus
mesacostalis, Hall, and fucoidal markings. The rocks in place near the sum-
mit of Bowie hill clearly belong in the lower part of the Ithaca formation.

The complete fauna is:

1. Spirifer mesastrialis, Hall. (c)
2. Spirifer mucronatus (Con.), Bill. (a)
3. Tropidoleptus carinatus (Con.), Hall. (a)
4. Liorhynchus mesacostatlis, Hall. (c)
5. Cyrtina Hamiltonensis, Hall. (1)
6. Chonetes setigera, Hall. (rv)
7. Rhynchonella (Camarotechia) Stevensi, Hall. (a)

Some of the smaller specimens more closely resemble 72. ex/mia,

Hall; but it is probable that the two forms blend into one species.

8. Atrypa reticularis (Linné), Dal. ar)
9. Actinopteria Boydi (Con.), Hall. (c)
10. Grammysia bisulcata (Con.), Hall (?). (rr)

SECTION OF MT. VISION AND BOWIE HILL.

715% | C4. Ithaca. Spiriter mesastrialis.
115° | Covered.

600! je -| C3 Sherburne (*).
250’ | Covered.

S19) bole te Bee C2, Hamilton.
250/ |

SOQ sets | C'!. Hamilton.

100° | Covered.

(oe ec | Otego creek level at Mt. Vision.

196 Report oF THE STaTe GEOLOGIST.

XXIV C°*. Along the outlet of Arnold lake, about 135 feet lower than
the top of Bowie hill, are quite fossiliferous bluish sandstones and shales.
Lower, along the highway to the southwest, are bluish thin shales with layers
of thin concretionary sandstones which contain specimens of Léorhynchus
mesacostalis, Hall, and Spiriter mucronatus (Con.), Bill. This fauna resembles
very closely the first of the Ithaca fauna as it appears at the top of the Sher-
burne formation, to which horizon these rocks are referred. The following
species were obtained from the bluish shaly sandstones at the outlet of the

lake and have been referred to the Ithaca fauna:

1. Liorhynchus mesacostalis, Hall. (c)
2. Spirifer mucronatus, (Con.), Bull. (c)
3. Spirifer mesastrialis, Hall. (c)
4. Grammysva elliptica, Hall. (11)
5. (¢) Terebratula (Hunella) Lincklaeni, Hall. (c)

The imperfect form in which these specimens are preserved
renders their identification difficult. Possibly they are narrow
specimens of Cryptonella Hudora, Hall.

Arnold lake is well surrounded by hills with steep banks, and the ice of
the glacial period probably excavated its basin.

C®, On the divide to the east of Arnold lake, from C’? and somewhat
higher, are thin olive shales and sandstones in which no fossils were found,
except fucoid markings. The lithologic characters of the rocks and the ab-
sence of fossils make this outcrop agree closely with those in the Sherburne
formation. ‘To the east is a very steep hill, dropping 300 feet into the valley
of Hinman Hollow brook; but, unfortunately, its flank is mostly covered
by drift.

XXV A‘. On the small divide between Hinman Hollow brook and a
small branch from the western side not over a mile to the northeast of Arnold
lake, and 290 feet below the divide at C®, are ledges of coarse, bluish, arena-
ceous shales containing Hamilton fossils in abundance. The outcrep is on the
north side of the road and is an excellent locality for collecting. There can

be no doubt in reference to the Hamilton age of these rocks. The fauna is:

lL. Athyris spiriferoides (Eaton), Hall. (a)
2. Cyrtina Hamiltonensis, Hall. (c)
3. Spiriter granulosus (Con.), Hall. (c)
4. Spirifer mucronatus (Con.), Bill. (c)
5. Spirifer fimbriatus (Con.), Bill. (c)

6. Chonetes scitula, Wall. (a)

ProssER—Haminron AND CHEMUNG SERIES. 197
7. Chonetes setigera, Hall. (r)
8. Ambocelia umbonata (Con.), Hall. (c)
9. Tropidoleptus carinatus (Con.), Hall. (c)
10. Zerebratula (Eunella) Lincklaent, Hall. (c)
11. Productella truncata, Hall (2). (11)
12. Atrypa reticularis (Linné), Dal. (rr)
13. Orthothetes Chemungensis (Con.), Hall and Clarke, var.
arctostriata, Hall. (c)
14. Microdon (Cypricardella) tenuistriatus, Hall. (c)
15. Chonetes coronata (Con.), Hall. (c)
16. Leda diversa, Hall. (1)
17. Paleoneilo muta, Hall. (1)
18. Nucula corbuliformis, Hall. (ar)
19. Modiomorpha concentrica (Con.), Hall. (ar)
20. Grammysia arcuata (Con.), Hall, (ar)
21. (2) Phthonia cylindrica, Hall. (117)
22. Pterinopecten Vertumnus, Hall (2). (17)
23. Coleolus tenuicinctus, Hall. (11)
24, Bellerophon, sp. (7)
Compressed specimens that have concentric and longitudinal
striae of about equal strength.
25. Cypricardinia indenta (Con.), Hall. (rr)
26. Spirifer Tullius, Hall. (rr)
27. Orthis Vanuxemi, Hall. (11)
28. Paleoneilo constricta (Con.), Hall. (r)
29. Phthonia sectifrons (Con.), Hall. (rr)
30. Schizodus appressus (Con.), Hall. (1r)
31. Glyptodesma erectum (Con.), Hall. (rr)
32. Microdon (Cypricardela) bellistriatus, Con. (?). (rr)
33. Nucula bellistriata (Con.), Hall. (1)
34, Liopteria DeKay?, Hall. (r)
Small and young specimens, like figure 10, plate 88 (Palaeon-
tology of New York, Vol. V, Part I).
35. Pleurotomaria capillaria, Hall. (rr)
36. Trilobite (fragment). ar)
37. Teniopora exigua, Nicholson. (c)

XXV <A®. Nearly one mile directly east of A’ on the high hill between

Hinman Hollow brook and the Susquehanna river, is another small glacial

198 Report oF THE STATE GEOLOGIST.

lake, known as Gowey or Little Pond. On the hill north of the pond and
145 feet higher, or over 500 feet above the Susquehanna river at Clintonville,
one and one-half miles to the southeast, are thin sandstones and bluish shales
that are unfossiliferous. They belong in the Sherburne formation which caps
the high hill between the Hinman Hollow brook and the Susquehanna river.

XXV A* On the divide to the east of Gowey pond, just at the be-
ginning of the descent into the Susquehanna river valley, argillaceous shales
with thin layers of blue sandstone show on the highway and in the field.
This outcrop is a little more than one mile southwest of Hartwick Seminary,
at an altitude of 400 feet above the Susquehanna river, and is typical Hamil-
ton, both in its lithologic appearance and its fauna, The following species
were collected :

1. Athyris spiriferoides (Katon), Hall. (c)
2. Tropidoleptus carinatus (Con.), Hall. (c)
3. Chonetes coronata (Con.), Hall. (c)
4. Spirifer mucronatus (Con.), Bull. (r)
5. Spirifer Tullius, Hall. (rr)
6. Ambocelia umbonata (Con.), Hall. (rr)
7. Chonetes scitula, Hall. (ar)
8. Orthis Vanuxemi, Hall. (rr)
9. (2) Crania, sp. ar)
10. Modiomorpha concentrica (Con.), Hall. (rr)
11. Chonetes lepida, Hall. (r)
12. Cypricardinia indenta (Con.), Hall. ar)
18. Nucula bellistriata (Con.), Hall. (c)
14. Leda diversa, Hall. (ar)
15. Schizodus appressus (Con.), Hall. (rr)

SECTION OF HILL NORTH AND EAST OF GOWEY POND.

510!) jan) AB Sherburne.
ANY: ilieearesnces A®. Hamilton.
400’ | Mostly covered.

Qo |...--| Level of Susquehanna river at Clintonville.

M

‘“NOLTINVYH YaddN SHL 3O SSIVHS NIHL SNIMOHS ‘ GYOITI) JO HLYON STIN ANO ‘'39H09 MOYUYUVN

09 GHOAMWYD HOIENSTIVH dOOMNAM

7

te

Se De ae

Wt S1W1d

we fi M5

a

.
i]
Y

HAMILTON AND CHEMUNG SERIES. 199

PRossER

In all this region between the Unadilla and Susquehanna rivers, the hills
are so mantled with the drift that it is frequently puzzling to determine
precisely where to draw the line of separation between different formations.
The streams in general afford the most satisfactory sections, although out-
cropping ledges on the sides of the steep hills sometimes furnish valuable

assistance.

Milford.

The township of Milford lies south of Hartwick and east of Laurens and
Oneonta. The Susquehanna river flows through the eastern part of the
township, to the east of which is a high and steep hill, while on the western
side the hill rises much more gradually and is broken by a number of small
valleys.

XXV 5'. In the northern part of the township is the village of Mil-
ford, and nearly one mile north of the village is a gorge along a small brook.
At the old mill the channel of the brook is narrow, with rock walls which
afford an excellent idea of the nature of the rather thin shales of the upper
Hamilton. The blue shales with which some thin sandstones alternate,
contain abundant specimens of Spirifer mucronatus (Con.), Bill., and the
complete list is:

1. Spirifer mucronatus (Con.), Bill. (a)
2. Chonetes lepida, Hall. (ir)
3. Tropidoleptus carinatus (Con.), Hall. (rr)
4. Paleoneilo fecunda, Hall. (17)

XXV BL. At the upper end of the short gorge, just below the highway
bridge, are bluish argillaceous shales in which Hamilton fossils are abundant.
The locality is about thirty feet above B! and perhaps 130 feet above the
hotel in Milford. This is a good locality for collecting, and. the following

species were obtained in a short time:

1. Spirifer mucronatus (Con.), Bill. (az)
2. Chonetes setigera, Hall. (aa)
3. Chonetes lepida, Hall. (c)
4. Tropidoleptus carinatus (Con.), Hall. (c)
5. Chonetes scitula, Hall. (ir)
6. Orbiculoided, sy). (rr)
7. Nuculites triqueter, Con. (11T)
8. Schizodus appressus (Con.), Hall. (c)

9, Paleonetlo constricta (Con.), Hall. (rr)

200 Report oF THE STATE GEOLOGIST.

10. Microdon (Cypricardella) tenuistriatus (2), Hall.

11. Goniophora Hamiltonensis (Hall), Miller. (rr)
12. Nucula lirata (Con.), Hall. (11)
13. Grammysia arcuata (Con.), Hall. (r)
14. Cimitaria recurva (Con.), Hall. (7r)
15. Palwoneilo maxima (Con.), Hall. (rr)
16. Modiomorpha mytiloides (Con.), Hall. (rr)

17. Dalmanites (Crypheus) Boothi (Green), Hall. (ar)

XXV ©’. This station is located at the point where the “Gulf road ”
crosses the brook at the falls, one mile northwest of Milford, and about two
hundred and ten feet higher than the hotel. The rocks forming the falls are
coarse, arenaceous Hamilton shales, containing numerous specimens of Spirifer
granulosus (Con.), Hall and Clarke, together with other fossils usually found
in the coarser Hamilton shales. Along the highway just above the falls are
finer shales, in which only the smaller forms of fossils occur. The fauna is:

1. Spiriter granulosus (Con.), Hall and Clarke. (a)
2. Tropidoleptus carinatus (Con.), Hall. (c)
3. Chonetes coronata (Con.), Hall. (r)
4. Cyrtina Hamiltonensis, Hall. (1)
5. Spirifer fimbriatus (Con.), Bill. (1r)
6. Platyceras conicum, Hall (?). (rr)
7. Crinoid segments. (c)
8. Spirifer mucronatus (Con.), Bill. (1r)
9. Macrodon Hamiltonia, Hall. (1r)
10. Modiomorpha concentrica (Con.), Hall. ar)
11. Microdon (Cypricardella) tenuistriatus, Hall (2). (tr)
12. Nucula corbuliformis, Hall. (1r)
13. Mytilarca (Plethomytilus) oviformis (Con.), Hall. (7)
14. Aviculopecten princeps (Con.), Hall (2). ar)
15. Pleurotomaria capillaria, Con. (1r)
16. Coleolus tenuicinctum, Hall. ar)

XX V J, Exposures along a small brook one and one-quarter miles
southwest of Milford, to the north of the Edson’s Corners road, and 195 feet
above the Susquehanna river at Portlandville. Moderately coarse shales con-
tain numerous Hamilton fossils, and the rocks are unhesitatingly referred
to the Hamilton formation. The fauna is:

1. Tropidoleptus carinatus (Con.), Hall. (1) -

2. Chonetes coronata (Con.), Hall. (ar)

PLATE IV

SHERBURNE SHALES ON HILL ONE MILE SOUTHWEST OF MILFORD

4 F ’ =
i ae tae ; bg
ae Te | .
< 3 t ' (
. 4 ae
“¥ 5 = = i =
eee S. é
. s 3 ‘
- 4 F i
AL as ‘ ‘ ,
i .
4 ; " : qv
- t he - + ; '
. = wT
= 7 > - A ~ j

ProssEr—Haminron AND CHEMUNG SERIES. 201

. Chonetes setigera, Hall. (1")
4. Nucula corbuliformis, Hall. (rr)
5. Nucula bellistriata (Con.), Hall. (1)
6. uculites triqueter, Con. (Gia)

7. Leda diversa, Hall. (1r)
8. Ambocelia umbonata (Con.), Hall. (rr)

9, Pleurotomaria captllaria, Con. (rr)

XXV /P*. In the field to the north of the brook and 225 feet higher,
or 420 feet above the river, is a ledge of arenaceous shales and thin sand-
stones. The shales are partly thin and even-bedded, similar to the Sherburne,
and unfossiliferous, with the exception of a layer possibly one inch thick.
The thin layer in which the fossils occur is largely composed of specimens
of Spirifer. A few of these are quite large, with the form and conspicuous
fine striae of Spirifer mesastrialis, Hall; but the majority of them approach
in form, nearer to Spirifer Tullius, Hall. These were the only fossils found
at this exposure, and, as far as observed, were confined to the one-inch layer,
I am inclined to regard them as representing the first of the Ithaca fauna
appearing in rocks that are synchronous with the upper part of the Sher-
burne formation in the Chenango valley.

-On the river road, one mile south of the point at which the Edson’s
Corners road joins it, are bluish shales that contain some Hamilton fossils.
At this locality these shales are some sixty feet above the Susquehanna river
level. The top of the Hamilton is considered to pass beneath the river level
in the vicinity of Portlandville.

XXII E*. Short gorge in small brook just northwest of Milford Centre,
about one and one-quarter miles southwest of Portlandville, or five miles
southwest of Milford. In the glen, forty-five feet of shales and thin bluish
sandstones are well exposed, and afford a good illustration of the unfossilifer-
ous Sherburne rocks of the Susquehanna valley. In some of the blue,
arenaceous, thin sandstones are fucoidal markings very similar in shape and
general appearance to those figured by Vanuxem and Hall as /wcordes
graphica, Van., from the Portage of central and western New York.

XXIT HE. In the brook at the upper bridge and ten feet above the top
of the gorge, are bluish, quite fossiliferous, rather arenaceous shales that con-
tain the lower Ithaca fauna, Spirifers occurring in several layers. The
locality is approximately 200 feet above the Susquehanna river level at
Portlandville, which would indicate a thickness of at least 200 feet for the

Sherburne formation in the Susquehanna valley. The fauna is:

202 Report oF THE STaTE GEOLOGIST.

1. Spirifer mucronatus (Con.), Bill. (a)
Long mucronate specimens.

2. Chonetes setigera, Hall. (aa)
Typical specimens.

3. Palewoneilo emarginata (Con.), Hall. (ir)

4. Grammysia elliptica, Hall (2). (11)

Dy Liorhynch us mesacostalis, Hall. (1r)

6. Segments of small Crznoid stems. (a)

SECTION OF THE MILFORD CENTRE GLEN.

2900p =e E*?. Jthaca.

1K Gy!
190" {ee
45° |) EX Sherburne of glen.
TADS |e ;
| 145’ | Covered.
|
0’ _| Susquehanna river level at Portlandville.

NNXIT EH. On the river road, about two miles south of Milford Centre,
or one-half mile north of Colliersville, are bluish shales by the side of the
highway. This exposure is eighty feet higher than the Delaware and Hudson
railroad at South Milford. Most of the rock consists of thin, blue, arenaceous
shales, like those of the Sherburne formation, although a few fossils, small
specimens of Spirifer mucronatus (Con.), Bill., and two imperfectly preserved
specimens of Chonetes scitula, Hall, were found. On the hill to the north-
east of South Milford, in the edge of Maryland township, are exposures of
the Sherburne sandstones some 140 feet higher than the South Milford
railroad station.

XX V 4. Crossing the Susquehanna river at Portlandville, the line of
division between the Hamilton and Sherburne was followed northeasterly along
the western slope of the steep Crumhorn mountain, About one and one-half
miles southeast of Milford, and below the corner of the road for Crumhorn
lake, are ledges of rather coarse, arenaceous Hamilton shales on the side of the
hill, perhaps 150 feet higher than the river. These shales contain a character-

istic Hamilton fauna, as may be seen from the following list :

LATE V

P

uy

\*

©
a4
oO
uw
=
As
&
oO
x
oO
Ww
[eal
Zz
Lub
ral
p=
=a
x
a
Oo
o
x
=
=

GROUP,

ITHACA

THE WHITE QUARRY WEST OF ONEONTA

PRrossER—HAMILTON AND CHEMUNG SERIEs. 203

1. Spiriter granulosus (Con.), Hall. (c)
2. Spirifer mucronatus (Con.), Bill. (c)
3. Spirtter Tuilirss, Hall. (11)
4. Chonetes coronata (Con.), Hall. (c)
5. Tropidoleptus carinatus (Con.), Hall. (a)
6. Stropheodonta demissa (Con.), Hall (?). (rr)
7. Orthothetes Chemungensis (Con.), Hall and Clarke. (rr)
8. OCyrtina Hamiltonensis, Hall. (rr)
9. Terebratula (Bunella) Lincklaeni, Hall. (rr)

About opposite Milford village, the Cherry Valley creek enters the Sus-
quehanna river from the east. The top of the Hamilton follows the western
side of Crumhorn mountain, on the eastern side of Cherry Valley creek, to the
northeast into Westford township. In the brook southeast of Westville
village, 420 feet above it and five and one-quarter miles northeast of Milford
village, are bluish shales containing plenty of Hamilton fossils and belonging
to the Hamilton formation. The fauna is:

1. Spirifer Tullius, Vall. (1)
2. Spirifer mucronatus (Con.), Bill. (1r)
3. Chonetes coronata (Con.), Hall. (ar)
“4. Chonetes scitula, Hall. (ar)
5. Chonetes setigera, Hall. (rr)
6. Ambocelia umbonata (Con.), Hall. (1r)
7. Crania Hamiltoniw, Hall (2). (1r)
8. Nucula bellistriata (Con.), Hall. (11)
9. Grammysia (Sphenomya) cuneata, Hall. (rr)

In the upper part of the “Gulf,” about one and one-half miles east of
Westville, 560 feet above the village, are even shales and thin sandstones that
are apparently unfossiliferous and belong in the Sherburne formation. Loose
specimens contain Zyopidoleptus cerinatus (Con.), Hall. The top of the hill
is some 900 feet above Westville village.

XXV G'. The top of the Hamilton follows around the side of the
steep hill to the northeast of Westville, and is crossed by the hill road wind-
ing down the steep northeastern side toward Westford village, about two and
one-half miles from Westville. The upper part of the hill is composed of the
arenaceous shales and thin sandstones of the Sherburne formation ; but on the
road, 525 feet above the valley of Elk creek, two miles below Westford, are

bluish argillaceous shales which break into rather small pieces and contain

204 Report oF THE STATE GEOLOGIST.

specimens of the smaller Hamilton fossils. The following species were
collected :

1. Chonetes scitula, Hall. (rr)

2. Spiriter mucronatus (Con.), Bill. (rr)

3. Tropidoleptus carinatus (Con.), Hall. (ar)

4. Orthis Vanuxemi, Hall. (r)

5. Nuculites triqueter, Con. (1r)
Maryland.

This township lies to the east of Milford and south of Westford town-
ships. Topographicaily it consists of very steep high hills separated by narrow
valleys, giving the township a very rugged surface. Along its western side
is Crumhorn mountain, a steep and high hill, while Schenevus creek flows
from the northeast to the southwest diagonally across the township, and
south of it is another steep hill.

XXIT C*. A ledge of thin argillaceous shales is excellently exposed
by the side of the street in the northeastern part of the village of Schenevus,
to the east of Smoky Hollow brook. The road-cut reveals twenty feet of
the shales, the base of which is perhaps 120 feet above the level of Schenevus
creek, The shales have rather sharp edges, are of very dark blue to blackish
color, and in lithologic characters resemble quite closely the thin shales of the
Ludlowville and Moscow divisions of western New York, or the so-called
“Genesee shales” (which are of upper Hamilton age) in northeastern Penn-
sylvania.’

These shales contain an abundance of characteristic Hamilton fossils and
furnish one of the best localities for collecting noted in the eastern part of
Otsego county. The following species were obtained :

1. Spiriter granulosus (Con.), Hall. (r)
2. Spiriter mucronatus (Con.), Bill. (c)
3. Spirifer Tullius, Hall. (c)
A. Spiriter fimbriatus (Con.), Hall. (1r)
5. Athyris spiriteroides (Katon), Hall. (c)
6. Chonetes coronata (Con.), Hall. (c)
7. Ambocelia umbonata (Con.), Hall. (c)
8. Tropidoleptus carinatus (Con.), Hall. (a)
9. Cyrtina Hamiltonensis, Hall. ar)

1 See Bulletin No. 120, United States Geological Survey; The Devonian system of eastern Pennsylvania and New York, pp.
36, 71, etc., for a discussion of the correlation of the fossiliferous shales in northeastern Pennsylvania.

ProsseER—Haminton AND CHEMUNG SERIES. 205

10. Cryptonella (Bunella) Lincklaeni, Hall. (1r)
11. Orbiculoidea Doria, Hall (2). (1)
Dorsal valves very convex with high apex. Rather large for
this species.

12. Crania (Craniella) Hamiltonie, Hall. (rr)
13. Nucula bellistriata (Con.), Hall. (a)
14. Nucula corbuliformis, Hall. (1)
15. Nuculites triqueter, Con. (c)
16. Nuculites oblongatus, Con. (c)
17. Nucula lirata (Con.), Hall. (1r)
18. Paleoneilo muta, Hall. (rr)
19. Paleoneilo constricta (Con.), Hall. (c)
20. Leda diversa, Hall. (c)
21. Leda rostellata (Con.), Hall. (ar)
22. Microdon (Cypricardella) bellistriatus (Con.), Hall. (aa)
23. Modiomorpha subalata (Con.), Hall. (c)
24. Grammysia bisulcata (Con.), Hall. (1)
25. Tellinopsis subemarginata (Con.), Hall. (ar)
26. Phthonia sectifrons (Con.), Hall. (11)
27. Prothyris lanceolata, Hall. (11)
28. Modiella pygmea (Con.), Hall. (17r)
29. Macrodon Hamiltoniw, Hall. (c)
30. Orthonota (2) parvula, Hall. (11)
31. Modiomorpha mytiloides (Con.), Hall. (ar)
32. Goniophora Hamiltonensis, Hall. (ar)
33. Orthonota carinata, Con. (17T)
34. Orthonota undulata, Con. (Ga)
35. Schizodus appressus (Con.), Hall. wera G 9
36. Lingula densa, Hall (2).

37. Hyolithes aclis, Hall. (1)
38. Coleolus tenuicinctum, Hall. (c)
39. Liopteria DeKay?, Hall. (ar)
40. Pleurotomaria capillaria, Con. (rr)
41. Cf. Wurchisonia micula (Hall), Miller. (11)

Imperfect internal impressions, only five volutions seen, but
evidence of carina on centre of body whorl.

42. (2) Psilophyton princeps, Dn. (ar)
43. Orthothetes Chemungensis (Con.), Hall, var. arctostriata, H. (rr)

206 Report OF THE STATE GEOLOGIST.

44. Paleoneilo emarginata (Con.), Hall. (ir)
45. Chonetes scitula, Hall. (ar)
46. Chonetes setigera, Hall. (1r)

NXAXIT ©. On the Schenevus creek road, one and one-half miles below
C*, or about one-half mile east of Chaseville, is another outcrop of dark blue
and blackish finely arenaceous shales of the Hamilton formation, contaiming an
abundant fauna. The ledge is from twenty to twenty-five feet high, about
ninety feet lower than C’, and thirty feet above the creek level. This ledge
shows a dip of more than 10° 8. 57° W., which means a dip in that direction

of over one hundred feet per mile. The fauna is as follows:

1. Spirifer granulosus (Con.), Hall. (c)
2. Spirifer mucronatus (Con.), Bill. (1)
3. Spiriter fimbriatus (Con.), Bill. (1r)
4. Chonetes carinata (Con.), Hall. (c)
5. Spirifer Tullius, Hall. (r)
6. Tropidoleptus carinatus (Con.), Hall. (17)
7. Athyris spiriferoides (Katon), Hall. (c)
8. Tellinopsis subemarginata (Con.), Hall. (11)
9. Orthis Vanuxemi, Hall (2). (rr)
10. Chonetes lepida, Hall. (7)
11. Cryptonella (Hunella) Lincklaeni, Hall (2). ar)
12. Palewoneilo maxima (Con.), Hall. (rr)
3. Paleoneilo constricta (Con.), Hall. (1)
14. Ambocelia umbonata (Con.), Hall. (rr)
15. Nuecula bellistriata (Con.), Hall. (c)
16. Leda diversa, Hall. (c)
17. Nuculites triqueter, Con. (17)
18. Nuculites oblongatus, Con. (ar)
19. Palewoneilo muta, Hall. ar)
20. Microdon (Cypricardella) bellistriata, Con. (17)
21. Schizodus appressus (Con.), Hall. | (1r)
22. Pleurotomaria captllaria, Con. (1r)
23. Lingula (Dignomia) alveata, Hall (?). (1T)

XXII [South of the Schenevus creek, opposite Schenevus village, is
a steep hill, on the side of which, along the highway and a small brook, are
frequent exposures. The lower part of the hill is composed of bluish-black

regular shales that contain Hamilton fossils, and belong to that formation.

“SNASNAHOS LY SSIVHS NOLMIANVH SHEL

IN. 3LVd

These

ProsseER—HaAmInTon AND CHEMUNG SERIES. 907

shales extend up the hillside 185 feet higher than the level of the

railroad. Near the foot of the hill they are quite fossiliferous, the following

species

LO:
Ef.
12.
hee

having been obtained :
Spirifer Tullius, Hall.
. Microdon (Cypricardella) bellistriata (Con.), Hall.
. Modiella pygmea (Con.), Hall.
Tropidoleptus carinatus (Con.), Hall.
. Nuculites oblongatus, Con., var.
. Phacops rana (Green), Hall.

Orthoceras calamen, Hall.

. Rhodea pinnata, Dn.

Spirifer mucronatus (Con.), Bill.
Grammysia subarcuata, Hall.

Chonetes coronata, Con.

Paleoneilo emarginata (Con.), Hall (?).
Nucula corbuliformis, Hall (2).

At nearly the top of the Hamilton shales, by the side of the highway,

the foll
ie

2,
2
4,

D.

owing species were collected :

Vitulina pustulosa, Hall. (c)
Tropidoleptus carinatus (Con.), Hall. (c)
Spiriter Tullius, Hall. (1)
Chonetes coronata (Con.), Hall. (rr)
Microdon (Cypricardella) tenuistriatus, Hall. (1r)

AXIT I?. Above the Hamilton are 175 feet of thin sandstones alternat-

ing wit

h greenish argillaceous shales. These rocks belong in the Sherburne

formation. No fossils were found.
XXII J*. Just above the even shales of J? is an irregular layer that

contains clay pebbles of various forms and some fossils, the species mentioned

below having been obtained :

if

o

—s

o

Spiriter Tullius, Hall. (1)
Tropidoleptus carinatus (Con.), Hall.

Leda diversa, Hall. (1°)
Microdon (Cypricardela) tenwistriatus, Hall. (17)
Paleoneilo constricta (Con.), Hall (2). (1r)

Modiomorpha cf. subalata (Con.), Hall, var.
Chemungensis, Hall. (rr)
A larger and longer specimen than any of the figures of the

above species.

208 Report oF THE STATE GEOLOGIST.

A little higher on the highway is quite a prominent concretionary sand-
stone, like the strata noted at other localities in the Ithaca formation. This
fauna and irregular lithologic structure occur at what may be considered the
base of the Ithaca formation in this section. About sixty feet above its base
by the roadside is an old stone quarry, which has been worked to some
extent for building stone. The shaly partings are quite fossiliferous, and
several good specimens of Spirifer mesastrialis were found. The fauna and
stratigraphic position of this zone are considered to indicate that it clearly
belongs in the Ithaca formation as it is developed in the eastern part of

Otsego county. The species mentioned below were collected here :

Spiriter mesastrialis, Hall. (c)

2. Paracyclas lirata (Con.), Hall. (1r)
3. Tellinopsis subemarginata (Con.), Hall. (ar)
4. Nucula bellistriata (Con.), Hall (rv)
5. Actinopteria Boydi, Con. ()
6. Actinopteria zeta, Hall (?). (r)
7. Pleurotomaria capillaria, Con. (c)
8. Paleoneilo emarginata (Con.), Hall. (rr)
9. Chonetes setigera, Hall. (rr)
10. Spirifer mucronatus (Con.), Bill (?). (r)
11. Pterinopecten suborbicularis, Hall (2). (ar)
12. Phacops rana (Green), Hall. (r)
13. Grammysia subarcuata, Hall. (ar)

Somewhat above the quarry a stratum of thin sandstone was seen (Chee )

which contains some fossils; the following were obtained

1. Tropidoleptus carinatus (Con.), Hall. (r)
2. Spiriter mesastrialis, Hall. (rr)
3. Spirifer mucronatus (Con.), Bill. (ar)
4. Goniophora Hamiltonensis, Hall. ar)

XXII [*, At 260 feet above the quarry, or 680 feet above the railroad
level on the top of the hill by the schoolhouse, is the base of a greenish,
coarse-grained sandstone, which marks the base of the Oneonta sandstone.
This massive stone remains very near the surface, and large blocks of it lie on
the ground so that the country for one mile to the south has a very rocky
appearance,

The above section for the hill south of Schenevus gives a thickness of
320 feet for the Ithaca formation and 175 feet for the Sherburne, or 495 feet
for the two;

)

and at the bottom more than 185 feet of the upper Hamilton.

PLATE VII

é
oO
w
@
=
te,
<>
=
a
o
So
=<
=
>
=

was

4

GENERAL VIEW OF THE SILVERNAILE QUARRY NORTH OF CHARLOTTEVILLE, SHOWING UPPER HAMILTON FLAGSTONES,

Prosser—HamintoN AND CHremuNG Series. 209

SECTION OF HILL SOUTH OF SCHENEVUS.

ACI a 4
735' Top of hill approximately 2,000 feet A. T.
55’. | It Oneonta.

G80) .=

260’ Tthaca.
420% Jone | T Quarry.

| 60!

Beil) | le I’. Layer with pebbles and fossils.

175’ | F Sherburne.
185’ per = Approximate top of Hamilton.

185’ | I’. Hamilton.

eee Railroad level at Schenevus 1,272 feet A. T.

XXII H'. To the north of Chaseville is a small brook, with steep hills
on both sides, that on the north rising over 900 feet above the level of
Schenevus creek at Chaseville. Near the top of the rock exposures in the
glen and about 215 feet above the creek level at Chaseville, are blue, argilla-

ceous shales containing Hamilton fossils. This outcrop belongs in the

Hamilton formation, and the following species were obtained :

L. Lropidoleptus carinatus (Con.), Hall. Ce)
2. Spiviter mucronatus (Con.), Bill. (11)
3. Chonetes setigera, Hall. (1°)
4. Orbiculoidea Doria, Hall (2).” (11)
5. Palwoneilo maxima (Con.), Hall. (rr)
6. Nueulites oblongatus, Con. (rr)
7. Nueula bellistiiata (Con.), Hall. (rr)
8. Phthonia sectifrons (Con.), Hall (2). (rr)
9. Palwoneilo constricta (Con.), Hall. QT)
10. Coleolus tenuicinctum, Hall. (11)
11. Bellerophon, sp. (1)

14

210 Reporr or tue Srare GRonoaist.

AN XI/ /7*, On the road along. the western side of the brook, 210 feet
above H}!, are thin, unfossiliferous sandstones and arenaceous shales resembling
the Sherburne formation in lithologic characters and probably belonging
to it. <A little higher, a concretionary stratum crosses the road; while at 582
feet above the creek level, or 157 feet higher than the lowest exposures of H?,

sandstones similar to those of the Sherburne are exposed on the road.

NXIT FH. On the road almost at the summit of the divide, two miles
north of Chaseville and twenty-three miles northwest of Schenevus, are argil-
laceous shales and shaly sandstones at an elevation of over 850 feet above
Schenevus creek. Spirifer mesastrialis, Hall, occurs abundantly in certain
layers of these shales, and they are unhesitatingly referred to the Ithaca for-

mation. The outcrop is a small one, but afforded the following species :

1. Spirifer mesastrialis, Hall. (a)
2. Rhynchonella eximia, Hall. | (c)
3. Goniophora, Spx. ar)
4. Pleurotomaria ct. rotalia, Hall. (c)

NNXIT H*, On the hillside north of the road and fifty feet higher than
H?, are plenty of arenaceous shales and thin sandstones containing an abun-
dance of the species which occur in the Ithaca formation of Otsego county.
The rocks closely resemble those that are found on the hill west of Oneonta

above the White quarry, and contain a similar fauna. The species are:

1. Spirifer mucronatus (Con.), Bill. (a)
oH. Spirifer mesastrialis, Hall. (c)
3. Tropidoleptus carinatus (Con.), Hall. ar)
4. Chonetes setigera, Hall. (rr)
5. Rhynchonella eximia, Hall, or P. Stevensi, Hall. (c)
6. Nueula corbul formas, Hall. (a)
7. Paracyclas lirata (Con.), Hall. (ar)
8. Palwoneilo maxima (Con.), Hall. ar)
9. Nuculites cuneiformis, Con. * qr)
10. Tentaculites cf. attenuatus, Hall. (1)

NNIT H?*. On the top of this high hill, some 930 feet above the level
of Schenevus creek at Chaseville, and scarcely twenty-five feet above H*, is a
ledge of irregularly bedded, coarse-grained, greenish-grey sandstones resem-
bling in all respects the greenish-grey sandstones of the Oneonta formation in
the vicinity of Oneonta, and this stratum is regarded as forming the base of

that formation, and has been so indicated on the accompanying geologic map.

‘AMYVNO FIIVNYSANS SHL JO dv3SH dWNG

WIA SivId

ProssER—H amintron AND CHEMUNG SERIES. 211

The Chaseville section may be tabulated as follows:

SECTION OF XXII H.

930’ << | Oneonta sandstone on top of hill.
S356
Cie eee H*. Jthaca in field.
50’

Ci | eect ese H®. J/thaca m road.

bray
ee Covered.

139° = Sherburne.

iS ere | Concretionary stratum.
18’
BOD! |... | H*®, Sherburne.

210’ | Covered.
215’ | _| H'. Hamilton shales.

Oy coli eee ee Schenevus creek level at Chaseville.

The above section shows that north of Chaseville, the thickness of the
Sherburne and Ithaca formations is between 505 and 715 feet.

AXX/IT BG. On the south side of Schenevus creek, three-quarters of a
mile to the southwest of Chaseville, is a brook which affords a good section of
over 500 feet. In the lower part, and but a short distance above the high-
way, are thin, argillaceous shales, containing only a few fossils, among them
Tropidoleptus carinatus (Con.), Hall. A little higher, the shales are coarser,
blocky, and contain quite a number of Hamilton species. The lithologic
characters of the lower shales are nearer those of the Sherburne formation,

and the upper shales bear those of the Hamilton. The fauna is:

1. Tropidoleptus carinatus (Con.), Hall. (c)
2. Spirifer mucronatus (Con.), Bill. (r)
3. Lingula densa, Hall (2). (Tr)
4. Paleoneilo constricta (Con.), Hall. (11)
5. Palwoneilo muta, Hall. Ur)

~

3. Grammysia alveata (Con.), Hall (2). (rr)

Di REPORT OF THE STATE GEOLOGIST.

7. Leptodesma Rogersi, Hall. (r)
8. Liopteria De Kay, Hall. (ar)
9. Bellerophon acutilira, Hall (2). (1r)

The striae are coarser than those in the species represented in
} }

the figures,

XXII L°. The shales are more arenaceous than those of B', alternating
with thin sandstones. The rocks are of bluish color, and fossils are rare,

only three species being found :

1. Tropidoleptus carinatus (Con.), Hall. (c)
2. Spirifer mucronatus (Con.), Bil. (r)
3. Spirifer Tullius, Hall. (c)

XXII LB. Above the first fall is a rather thin, somewhat coarse-grained
sandstone, in which fossils are rare. In thin layers several specimens of
Liorhynchus were found, though poorly preserved. As a rule, however, the
rocks are quite destitute of fossils. The fauna of B? is:

1. Liorhynchus mesacostalis, Hall. (1)

2. Crania, sp. (c)

Poorly preserved, possibly C. Zeont, Hall.
3. (2) Cryptonella Hudora, Hall. (11)

XXII LB Thin, blue-grey sandstones and arenaceous. shales, which
contain numerous specimens of Spirifer mesastrialis, Hall; Spirifer
mucronatus (Con.), Bill.; Zopidoleptus carinatus (Con.), Hall, and other
fossils. These sandstones are near the top of the hill, nearly 500 feet
above the level of the creek and are clearly in the Ithaca formation. The

fauna is:

1. Spirifer mesastrialis, Hall. (a)
2. Spirifer mucronatus (Con.), Bill. (c)
3. Tropidoleptus carinatus (Con.), Hall. (c)
4. Chonetes scitula, Hall. (a)
5. Rhynchonella (Camarotechia) eximia, Hall. ar)
6. Rhynchonella (Camarotechia) Stevens’, Hall. (r)
7. Liorhynchus mesacostalis, Hall. (ar)
8. Nucula bellistriata (Con.), Hall. (ar)
9. Palwoneilo constricta (Con.), Hall. (ar)
10. Leptodesma Rogersi, Hall (?). (1)

11. Actinopteria, sp. (rr)

‘NOSYHY34S43f JO HLMOS ANOLSGNVS VLNOSNO SHI JO 3SVq

X| 3LW1d

OL am

ProssErR—Haminton AnD CHEMUNG SERIES. 213

SECTION OF XXII B.

600’ |~. Near the summit of the hill.

| 1107 | Ithaca.

490’ |... B£ Sandstones with Spiriter mesastrialis,
140’
A Saaeees | Coarse-grained sandstones.
120’
50 coos — B®. Sandstones with Léorhynchus.
Ah? |
MD [eae iB Small Spiriferd.
yay |
130’ |... B'. Shales with Hamilton fossils.
1307 |
Dee 2h | Level of Schenevus creek.

XXII 4°. On the road leading over the steep hill south of the village
of Maryland are, toward the summit of the hill, exposures of the Ithaca forma-
tion. One at an elevation of 470 feet above the creek level at Maryland, con-
tains numerous species of the Ithaca fauna, as will be seen from the list :

1. Spirifer mucronatus (Con.), Bill. (c)
Part of the specimens have decided mucronate extensions of the

shell and are typical.

2. Spiriter mesastrialis, Hall. (rr)
3. Zropidoleptus carinatus (Con.), Hall. (c)
4. Fhynchonella (Camarotachia) Stevensi,. Hall. (rr)
5. Phynchonella (Camarotechia) eximia, Hall. (1)
6. Chonetes scitula, Hall. (c)
7. Fragments of Gastropods. (4) Pleuwrotomaria, sp. ar)
8. Palwoneilo, sp. (rr)
9. Coleolus aciculum, Hall (4). (rr)
10. Orthoceras, sp. (rr)
11. Homalonotus DeKayi (Green), Emm. (1r)

ARG EA. Fifty feet higher, or 620 feet above the creek, near the
summit of the hill, are massive ledges of greenish-grey coarse-grained sand
stone, which form the base of the Oneonta sandstone. Judging from outcrops

to the north of the village of Maryland, the Hamilton formation runs along

214 Report oF THE Srare GEOLoGIs?.

the creek valley at this locality, so that the thickness of the Sherburne and
Ithaca formations in the hill to the south of Maryland is less than 600 feet.

XXII A. In the vicinity of Maryland village, two brooks enter Sche-
nevus creek from the north; Whitney brook, which flows through the eastern
part of the village, and Morehouse brook, about three-fifths of a mile farther
west. Their general direction is to the southwest, each side being flanked
by very steep hills. The hill forming the divide between them is especially
steep and narrow, and is known in that region as Little Crumhorn mountain.
Along Whitney brook, after reaching an altitude of seventy feet above Sche-
nevus creek, are frequent ledges. and cliffs of rocks until the upper part of its
course is reached. From these outcrops the following section along this brook
was constructed, the divisions being characterized as follows:

The first outcrop is seventy feet above Schenevus creek level, where a
stratum of blue sandstone (A*), two and one-half feet thick, crosses the brook.
No fossils were found, but it has the usual lithologic characters of the rather
heavy layers of Hamilton sandstone.

NXIT A®. For thirty feet above the first sandstone stratum there are
numerous outcrops of shaly sandstones, sbales and bluish sandstones along
the bed and banks of the brook about one-quarter of*a mile northeast of
Maryland village. Some of the beds are of typical Hamilton character, con-
taining a great abundance of Hamilton species, while others are thin, rather
even sandstones, with a greenish rather than bluish tint, resembling con-
siderably some of the Ithaca layers of Tompkins and Cortland counties.
Some of the layers containing abundant Hamilton fossils are of a very dark

color, almost black. The fauna is as follows:

1 Sporiter granulosus (Con.), Hall. (a)
2. Spirifer Tullius, Hall. ()
3. Cyrtina Hamiltonensis, Hall. (1)
4. Tropidoleptus carinatus (Con.), Hall. (c)
5. Modiomorpha concentrica (Con.), Hall. (rr
6. Phthonia sectifrons (Con.), Hall (?). (rr
7. Athyris spiriferoides (Katon), Hall. (rr)
8. Palwoneilo muta, Hall. (rr)
9 Grammysia bisuleata (Con.), Hall. (ar)

Loose on the highway to the west of the brook and higher than A*, the
following species were collected :
1. Nucula bellistriata (Con.), Wall. (1)

2. Palaoneilo constricta (Con.), Hall. (vr

'SQ3G NOLIINVYH YaddN ONIMOHS : NSagvWvaYg JO HIYON “WSSY9D AIYWHOHOS SH1L NO "NIVLNNOW VYIIVHAVAA SO LOOA

X 31V1d

é

a 1% i

ProssEr-—Hamintron AND CHrmMUNG SERIES. 915

3. Tropidoleptus carinatus (Con.), Hall. (r)

4. Athyris spiriferoides (Katon), Hall (4). (rr)

XXIT A*. At an elevation of one hundred feet, the bluish shales con-
taming an abundant Hamilton fauna are succeeded by greenish to bluish
unfossiliferous shales and thin sandstones. This zone is about seventy-five
feet thick and forms the bottom of the brook for some distance.

XXIT A®. At the top of these greenish rocks, and 175 feet above the
level of Schenevus creek, are blackish to bluish, sharp argillaceous shales,
some forty-five feet of which occur along the banks of the creek. They con-
tain plenty of fossils, the following list of species having been obtained in a

comparatively short time :

1. Spirifer granulosus (Con.), Hall. (c)
2. Spirifer mucronatus (Con.), Bill. (ar)
3. Spirifer Tullius, Hall. (ar)
4. Atrypa reticularis (Linné), Dal. (1)
5. Liorhynchus multicosta, Hall. (17)
6. Tropidoleptus carinatus (Con.), Hall. (c)
7. Chonetes mucronata, Hall. (rr)
8. Athyris ct. Cora, Hall. (rr)

One poorly preserved specimen, resembling this species more

closely than A. spiriferoides (Eaton), Hall.

9. Nucula bellistriata (Con.), Hall. (c)
10, Nucula corbulitormis, Hall. (1r)
11. Paleonetlo constricta (Con.), Hall. (rr)
12. Nuculites triqueter, Con. (7)
13. Nuculites oblongatus, Con. (ar)
14. Modiomorpha concentrica (Con.), Hall. (rr)
15. Schizodus appressus (Con.), Hall. (rr)
16. Modiomorpha mytiloides (Con.), Hall. (11)
1%. Microdon (Cypricardella) tenuistriatus, Wall (4). (rr)
18. Cyclonema Hamiltonie, Hall. (rr)
19. Orthoceras crotalum, Hall. (rr)

When this section was studied, the author was not positive whether the
top of zone A® should be considered the top of the Hamilton formation and
the abundant fossils of A® a recurrent Hamilton fauna in the Sherburne for-
mation, or whether the forty-five feet of zone A® should be referred to the
Hamilton. However, after examining the fauna of A?’ and comparing the
section with the others of that vicinity it seems better to consider the top of

216 Report oF THE Svavre (GEOLOGIST.

A? as the upper limit of the Hamilton. In the section to the north of Chase-
ville, which is one and one-half miles east of Whitney brook, the Hamilton
formation and fauna were found up to 215 feet above Schenevus creek. The
next 210 feet are covered, but it is probable that the Hamilton formation
extends considerably higher, since on the south side of Schenevus creek oppo-
site Schenevus and Maryland the combined thickness of the Sherburne and
Ithaca formations is about 500 feet, while it is 715 feet from the top of the
last Hamilton exposure in the brook north of Chaseyille to the bottom of the
Oneonta sandstone.

XXII A*. About twenty-five feet above the top of A®, is the foot
of a cascade at a distance of about one and one-quarter miles from the
village. The rocks are bluish argillaceous, and even arenaceous shales that
weather to a slightly olive tint. They contain but few fossils, though they
show plenty of fucoidal and mud markings. In this latter character and their
lithologic appearance they clearly resemble the Sherburne shales. Only frag-
ments of these fossils were found : ,

1. Spiriter cf. mucronatus (Con.), Bill. (rr)

2. Liopteria De Kayi, Hall. (11)

XXII A". The lithologic characters of the shales between the two falls
are quite similar to those below the falls, and they contain a few fossils. Ina
thin layer about ten feet above the top of the lower falls are a considerable .
number of specimens of Lingu/a. The complete list is:

1. Lingula punctata, Hall (%). (c)

The specimens are not quite as broad as the figures of this species,
except figure 6f, plate 1 (Palaeontology of New York, Vol. IV),

but the shell shows fine puncte.

2. Lropidoleptus carinatus (Con.), Hall. (rr)
3. Spirifer, sp. (ar)
Two small and imperfect specimens.
4. Nuculites triqueter, Con. ar)
5. Bellerophon, sy. (1r)
Fragments that have markings somewhat like those of . Leda,
Hall.
6. (2) Rhodea pinnata, Dn. (rr)

Stem like the above plant, except that the branching is alternate
instead of opposite as im that species.
XXII A*. Near the top of the second falls, 290 feet above the Sche-

nevus creek, are bluish, shghtly irregular shales, which contain a number of

“AATIVA AINVHOHOS ‘WISHNS1G HLYON LY T1IWLSS/A\ SHL NI MalA

OD CHOAMVYS HOIEBNITIVH. dOOMNAM

IX 31V1d

ProssER—Hamitron AND CuEemuNG SrErtres. DG

fossils. The fossiliferous layer is only about six inches in thickness, and

contains the following species :

1. Spirifer mucronatus (Con.), Bill. (1)
2. Spirifer mesastrialis, Hall (4). (rr)
3. Spirifer fimbriatus (Con.), Bill. (11)
4. Chonetes setigera, Hall. (it)
5. Chonetes lepida, Hall. (rr)
6. Stropheodonta ( Leptostrophia) cf. perplana (Con.), Hall. (1)
7. Lingula, sp. (rr)
8. Gontophora Hamiltonensis, Hall. (ar)
9. Paleoneilo constricta (Con.), Hall. (rr)

NX/II A*, Above the second falls the rocks are much more generally
covered by soil than below. In the occasional exposures of shales and sand-
stones for the next 130 feet an occasional specimen of 7/opidoleptus carinatus
(Con.), Hall, and one or two other species were noticed. At 420 feet above
Schenevus creek is a stratum of irregular sandstone, with partly concre-
tionary structure, similar to those which occur not infrequently in the upper
portion of the Middle and Upper Devonian in eastern central New York.
The structure of this stratum may be similar to that noted by Clarke in
Chenango and Ontario counties,! except that this is not stained red, inasmuch
as it is considerably below the lowest of the red rocks. Shales of bluish and
olive color occur both above and below the sandstone stratum. The shales
and sandstone contain a few fossils, Cyrtina Hamiltonensis, Hall, being abun-

dant ma thin layer. The other species collected are :

2. Spirifer mucronatus (Con.), Bill. (rr)
3. Tropidoleptus carinatus (Con.), Hall. (1)
4. Liorhynchus, sp. (1)

Small and imperfectly preserved specimens.

Fifteen feet above the concretionary stratum is a layer containing L/o-
rhynchus. For the next 195 feet to the east and west highway, the rocks are
mostly covered ; which is also true for the additional 185 feet when the top
of the divide between the Whitney and Morehouse brooks is reached. This
divide is approximately 815 feet above the level of Schenevus, or over 2,000
feet above sea level In this section the Ithaca formation is scarcely exposed,
the upper part of the brook and the hill slope being deeply covered by drift.

Spiriter mesastrialis, Hall, was found loose in the brook below the east and

218 Report oF THE STATE GEOLOGISY.

which fossils are not uncommon, in fact, they are more plentiful at this locality
than is the case in Chenango county and the western part of Otsego. The
Hamilton in the lower part of the valley contains plenty of Hamilton fossils,

though they are very rare in a zone in the upper part of the formation.

XXII A. SECTION OF WHITNEY BROOK NORTH OF MARYLAND.

Approximately 2,013 feet A. T.

rows 94
Top of Little Crumhorn mountain, between Whitney
| ;
leo and Morehouse brooks.
| 185 A’. Covered.
630! |---| KE, & W. highway.
|
O57 Ae Mostly covered,
435’ | | Lnorhynchus A*.
Pas
420’ |- Concretionary layer A’.
|
130’ A’, Largely covered.
990 | - Top of upper cascade.
A Nt
9457 |- | Foot of lower cascade.
25° AS Sherburne formation. ,
229()/ Top of layer with abundant Hamilton fossils.
AB) Ae
175’
75! A‘ Greenish shales and thin sandstones. a
100’ | Abundant Hamilton fossils. Ss
| ~
30’ Ae: ss
70! A®. Blue sandstone, two and one-half feet thick |
50’ at base of rocks.
7h a Railroad level, 1,218 feet A. T. A‘.
OKO!
(Oy Level of Schenevus creek.

PLATE XiIl

-ORDEO.

is
i
af
: Q

MINEKILL FALLS, SCHOHARIE VALLEY ; ITHACA BEDS,

ProssER—Haminton AND CHEMUNG SERIES. 219

XXIT D'. In the Morehouse brook at the lower end of. its

between 125 and 150 feet above the level of Schenevus creek, are arenaceous

vorge,
blocky shales containing an abundant Hamilton fauna. Higher in the gorge
are thin, even, sandy shales that closely resemble the Sherburne shales. The

lower part of the glen is clearly Hamilton, as may be seen from its fauna:

1. Spirifer mucronatus (Con.), Bill. (a)
2. Spirifer granulosus (Con.), Hall and Clarke. (c)
3. Tropidoleptus carinatus (Con.), Hall. (c)
4. Orthothetes Chemungensis (Con.), H. and C., var. arctostriata. (ar)
5. Atrypa reticularis (Linné), Dal. (rr)
6. Athyris spiriferoides (Katon), Hall. (11)
7. Paleoneilo muta, Hall. (ar)
8. Modiomorpha mytiloides (Con.), Hall. (rr)
9. Ambocelia umbonata (Con.), Hall. (rr)

10. Terebratula (Hunella) Linchlaeni, Halt. (rr)

220) Report oF THE STATE GEOLOGIST.
CONCLUSION.

On the g
Hamilton formation, and the Sherburne and Ithaca formations taken together

eologic map accompanying this report, the boundaries of the

are given for Chenango, Otsego, Schoharie, Albany and Greene counties. In
the preceding portion of this report detailed sections with lists of fossils are
given for Chenango and Otsego counties. It was intended to give a similar
account of the investigation in Schoharie, Albany and Greene counties, but
the pressure of other duties renders it necessary to defer their description until
a later date, when a summary of the more important facts brought out by this
investigation will appear. However, in order that the reader may apprehend
the more important changes advocated in the present report, it is thought best
to state them briefly.

On comparison it will be noticed that the line marking the upper
boundary of the Hamiiton formation on the geologic map is from five to fifteen
miles farther south than the similar line on the geologic map, recently pub-
lished by the Geological Survey of the State of New York.t

As stated in the introductory part of this paper, wherever the Tully lime-
stone is found, it affords a sharp line of separation between the Hamilton and
Chemung series; but in eastern and eastern central New York the Tully
limestone as well as the overlying black Genesee slate has disappeared and
there is a more gradual passage from the Hamilton to the Chemung series.
The author began work in De Ruyter, Madison county, where both the Tully
limestone and Genesee slates occur, and followed those formations into the
Chenango valley, where they disappear. In Onondaga, Cortland, Madison
and Chenango counties, above the Tully limestone and Genesee slate, are the
thin bluish sandstones and smooth shales of the lower Portage of central and
western New York, Vanuxem proposed the name “Sherburne flagstone ”*
for this formation, which has been adopted in this report, and it is shown to
have a thickness of 250 feet in the Chenango valley. In this valley and
the westward the Sherburne formation contains comparatively few fossils,
though to the east, after the disappearance of the Tully limestone and
Genesee slates, the number of species, particularly of Hamilton forms,
increases, as has been shown in the latter part of this report in describing the
exposures in the eastern part of Otsego county. However, when the sections

are carefully studied by one familiar with the Hamilton and Chemung series,

! Preliminary Geologic Map of New York, exhibiting the structure of the State so far as known. Prepared under the direc-_
tion of James Hall, State Geologist, by W. J. McGee. Published by authority of the Legislature of the State of New York.
Printed by the United States Geological Survey, 1894 (distributed April, 1896).

2 Fourth Annual Report, Third Geological District (Assembly Document No. 50, 1840), p. 381.

WYNKOOP HALEEN

PLATE XIII

MANORKILL FALLS, SCHOHARIE VALLEY, ABOVE GILBOA.

ONEONTA SANDSTONE,

bo

ProssER-—HAMILTON AND CHEMUNG SERIES. ey

almost invariably the change from the Hamilton to the Sherburne formation
may be readily determined even in the eastern part of the area under con-
sideration. On the geologic map prepared for this report, the Tully limestone,
and its horizon where it could be recognized, was regarded as defining the upper
limit of the Hamilton formation. On the geologic map of New York, the
upper line of the Hamilton is represented as crossing the northwestern town.
ships of Chenango county, Lincklaen, Otselic and Smyrna, several miles to
the south of the outcrops of the Tully limestone, which enters the county
near the northwestern corner of Smyrna township and was followed along the
southern side of Pleasant brook to Smyrna village. After the disappearance
of the Tully limestone the transition from the Hamilton to the Sherburne
formation was generally readily recognized, and this horizon as traced across
the eastern part of Chenango, Otsego, Schoharie, Albany and Greene counties,
is represented on the accompanying map as marking the upper limit of the
Hamilton formation. The above division of these rocks is confirmed palaeon-
tologically by the discovery of the characteristic Tully species, Rhynchonella
venustula, Hall, at this horizon in the central part of Otsego county.

Above the Sherburne formation is one, containing numerous fossils, that
may be followed westward from the Chenango valley across Chenango, Cort-
land and Tompkins counties to Ithaca, where it long ago received the name
“Ithaca group.”'! The Ithaca formation has a thickness of fully 500 feet in
the Chenango valley, and from there it may be traced eastward into Greene
county, which is apparently near the limit of its eastern extent. The upper
limit of the Ithaca formation is determined by the appearance of the coarse,
ereenish-grey and red sandstones and shales of the overlying Oneonta forma-
tion. On the present map, the Sherburne and Ithaca formations are repre-
sented together, the line already defined as representing the top of the Hamil-
ton indicating the base, and the line separating the Ithaca «and Oneonta
defining the top. On the geologic map of New York, from the Chenango
valley eastward, the base of the Oneonta sandstone was regarded as forming
the top of the Hamilton formation, the Ithaca and Sherburne formations being
mapped as a part of the Hamilton formation. Consequently, with some
modifications, the line representing the top of the Hamilton on the State
map will be found to correspond to the line on the accompanying map repre-
senting the top of the Ithaca formation. From what has just been said it will
be understood that on the State map from the Chenango valley eastward there

is no line corresponding to what the author regards as the line of division

1 Third Annual Report, Fourth Geological District, New York (Assembly Document No. 275, 1839), p. 318.

RD, Reporr or THE Srark GEOLOGIST.

between the Hamilton and Chemung series or, to express it more precisely,
between the Hamilton and Sherburne formations.

In the region under consideration, the field work directly preliminary to
the preparation of the geologic map of New York was conducted by Mr. N. H.
Darton, of the United States Geological Survey. Mr. Darton evidently
regarded all of the fossiliferous rocks underlying the Oneonta formation as
belonging to the Hamilton, and did not consider what became of the Tully
limestone, Genesee slate, Sherburne and Ithaca formations which, at Ithaca,
fifty miles west of Norwich in the Chenango valley, have a thickness of nearly
850 feet.

Mr. Darton first published an account of this work in March, 1893, in
which he stated that “* The stratigraphic components of the Oneonta forma-
tion are somewhat variable in its smaller subdivisions, but certain members
preserve general characteristics throughout. The basal beds are grey flags
which merge into the Hamilton.”' The same correlation was shown in his
figure 2 B through Oneonta and Franklin,? where the Oneonta is represented
as resting directly on the Hamilton. Again it is stated that “the Hamilton
is exposed” at the Lyon brook bridge*® in the Chenango valley, a locality
which has been described in this report as representing the top of the Ithaca
formation capped by the basal part of the Oneonta.

At an earlier date the writer published a paper* in which was traced the
development of the classification of the Upper Devonian system in central and
eastern New York. The error of correlating the fossiliferous beds below the
Oneonta sandstone in the Chenango and Susquehanna valleys with the upper
Hamilton was fully explained, both the stratigraphic and palaeontologic evi-

dence being given.

1 American Journal of Science, Third series, Vol. XLV., p. 206.

2 Thid., p. 205.

% Loc. cit., p. 207.

4 The Upper Hamilton and Portage stages of central and eastern New York. American Journal of Science, Third series, Vol.
XLVL., Sep. 1893, pp. 212-231.

GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

THE SERATIGRAPHIC POSITION OF .THE PORTAGE SAND-
STONES IN THE NAPLES VALLEY AND THE
ADJOINING REGION.

JAMES HALL, DAN AS UE,

State Geolog ist, | Assistant.

1895,

James Hani, State Geologist.

Str:—I herewith submit a brief account of the geology of the Naples
valley, designed to show in some detail the nature of the Portage section
in that meridian, and the stratigraphic relations of the. upper beds, originally
termed the Portage sandstones.

Respectfully yours,
D. DANA LUTHER.
Napiss, N. Y., March 28, 1896.
225

15

‘SAIdWN ‘ATIND SAWIND ‘Wd GYIHE

} a1W1d

The Stratigraphic Position of the Portage Sandstones in the
Naples Valley and the Adjoining Region.

By D. Dana LurueEr.

The deep wells that have penetrated the great beds of rock salt lying at
varying depths below the surface of a large section of country in western and
central New York, have demonstrated that the northern limit of these beds is
approximately the line of outcrop of the Corniferous limestone, thé top of
which is but little more than 500 feet above the salt horizon.

South from this line, owing to the dip of the strata and the generally
mcreased elevation of the surface, deeper drilling is required, as the strata that
compose the Marcellus, Hamilton, Genesee, Portage and Chemung groups are
successively added to those that intervene between the surface and the salt.

In the Warsaw or Oatka valley, in Wyoming county, the sandstones at
the top of the Portage group are a little more than 2,000 feet above the salt.
This distance increases slightly toward the east, and more rapidly toward the
south.

Nearly all of the deep north and south valleys that are so numerous in
this section of country, have been excavated in the soft shales of the Hamilton,
Genesee and Portage groups, and end at the south in the harder and heavier
bedded Upper Portage and Chemung sandstones, Although the salt beds are
known to increase in thickness toward the south, those reached by the wells in
these valleys have been found abundantly sufticient for all purposes, and but
two plants, the Duncan Salt Co.’s, at Silver Springs, and that at Castile, have
been put into operation where the stratigraphic horizon of the mouths of the
salt wells is above the top of the Portage sandstones, and in those wells the
thickness of Chemung rock included in the sections is not great.

As these “ Portage sandstones,” so designated on account of their great
development and abundant exposure at the upper Portage falls, on the
Genesee river, and described by Professor Hall in the Report on the Geology
of the Fourth District, 1848, can be easily identified by any careful observer,
and are fairly persistent in character from Tompkins county to the shores of
lake Erie, their line of outcrop may, for the reasons previously mentioned, be

considered as marking the southern limit of that part of the salt-producing

997

lo
lo
t

Report OF THE STATE GEOLOGIST.

area of central and western New York, that is profitably accessible for com-
mercial purposes.

In order to show the position of the Portage sandstones in the strata and
their relations to the geologic divisions above and below them, the rock
section in a typical valley of the “finger lake region” lying in the extreme
southern part of Ontario county, and in the central part of the New York
salt fields, the valley of Naples, is here given.

The valley of Canandaigua lake extends about five miles beyond the
head of that lake in a southwesterly direction, to the southern boundary line
of the town of Naples, Ontario county. It has an average width of about one
mile. The sides are steep and high. Hatch hill on the east side rises to the
height of 1,041 feet above the lake level, and Pine hill at the south, and High
point, one mile west of the valley, are each about two hundred feet higher.

The floor of the valley for three and one-half miles from the lake is a low
alluvial plain, but at the south end there is an immense deposit of morainic
till, and the delta terrace at the mouth of Grimes gully, nearly 200 feet high,
projects half way across the valley. The village of Naples is situated at the
foot of this terrace.

On the steep hillsides the soil, which is composed largely of the disinte-
grated shales, is thin, and loose fragments removed but slightly from their
original position in the harder sandy layers, abound everywhere. The dug-
ways ascending the hills diagonally, frequently afford long exposures of the
bed rock, but the best opportunities for examination of the rock strata are
presented in the ravines or gullies, of which there is a large number
debouching into the main valley. The largest of these is the Parrish gully,
on the east side, about two miles south of the lake. An alluvial cone at the
mouth is about fifty feet higher than the lake. Above the cone the bottom
and sides of the ravine present an interesting and accessible rock section
somewhat less than 600 feet high, that includes all of the strata of the Portage
group except some shale beds at the base.

The Tannery gully, also on the east side, but near the south end of the
valley, exposes a continuous section 500 to 600 feet thick, beginning in the
middle Portage or Gardeau fiags, and extending upward into the Chemung
sandstones.

On the west side, the Grimes gully exposes about 400 feet of the upper
Portage and lower Chemung rocks. The Portage sandstones are particularly
well displayed in this ravine and present abundant opportunity for the most ~

critical examination.

LutHEr—PortacrE SANDSTONES. 229

The three ravines above specified are veritable canyons with vertical
rock walls, 100 to 200 feet high, and many beautiful cascades. Besides these
there are many others but little less extensive, in which there may be founda
good exposures of every horizon of the Portage group, and which have at
their mouths alluvial cones composed of the debris brought down by the
streams flowing through them.

The more important named in order from the lake southward, are the
Snyder, Hartman, Biehl, Yaw, Pottle, Dunton, Lincoln and Hoecker gullies
on the west side, in which the lower and middle Portage beds are exposed,
and the Caulkins, Tyler and Reservoir or Olney gullies in the upper Portage
and lower Chemung. Although no single exposure gives a continuous section
from undoubted Genesee to undoubted Chemung rocks, the outcrops are so
numerous that, as the strata persistently maintain their individual character,
which can usually be easily recognized by the careful observer, it is not difficult
to join the sections with comparative accuracy.

This report and the diagram accompanying it are the result of examina-
tions and measurements made at all of the best exposures in the valley.

The contact with the Genesee slate at the base of the Portage
group, 1s not distinctly marked, and any dividing line established between
these two divisions must necessarily be, in this locality, a somewhat arbi-
trary one.

At the head of Canandaigua lake, near the Woodville hotel, there is an
exposure that embraces fifty to sixty feet of typical upper Genesee slate, soft,
dark blue-grey, in which Zunulicardium fragile and other characteristic
fossils are abundant.

By the side of the road leading southward toward the village of Naples,
the upper layers of the same bed are exposed for a quarter of a mile, to the
mouth of the Snyder gully. In this ravine the dark slaty shales are overlaid
by about fifteen feet of soft, clayey, olive shales that contain a few fossils
common to the Portage group, but Z. fragile is still the most abundant form.
These beds were termed by Clarke, “transition shales,” and may properly be so
considered, as there is no recurrence of the Genesee slates, and LZ. fragile is
very rarely seen above them. Next above occur fifteen feet of dark slaty and
lighter sandy shales, in which are intercalated a few thin flags, in which the
proportion of dark shale increases toward the top, where the lighter layers
disappear and a bed of densely black, bituminous fissile shale about fifteen feet
thick is found, overlaid by fifteen feet of black and grey shale of the same

character as those below the bituminous layer. Plant remains are common

930 Report oF THE Srateé GEOLOGIST.

_ here, and fish scales and plates are sometimes found, Other fossils appear to
be very rare in these beds.

These forty-five feet constitute what has been termed the Lower Black
Band of the Portage group, and the contact line between the Portage and
Genesee groups is, In this report, assumed to be at the top of the transition
shales before mentioned, and at the base of this black band. Directly above
there are seventy-six feet of bluish or olive, sandy shales and very soft and
thinly laminated sandstones with occasional flags. Both shales and sandstones
are almost entirely devoid of traces of life except for the object known as
Fucoides graphica, and some undeterminable plant remains. Six feet of blue
sandstones overlie these barren shales, above which the recurring olive shales
are softer and argillaceous.

This latter bed of shale is seventy feet thick, the lower part nearly barren
of fossils, but the upper layers contain in some abundance Cardiomorpha
suborbicularis and Cardiola retrostriata, while several species of goniatites and
other characteristic forms are common. The composition of the strata changes
very frequently in the succeeding 150 feet, and embraces thick and thin blue
and grey sandstones and blue, olive, grey and black shales in thin beds. Con-
cretions and concretionary layers also occur, with one highly concretionary
layer of impure limestone about four inches thick. Fossils are fairly
abundant in these beds at nearly every horizon, and many new and interest-
ing forms have been found in them during the last few years. Near their
top is a bed of black shales twenty feet, nine inches thick, known as the
Second Biack Band. Its summit is 287 feet above the base of the group.

This second black band is overlaid by forty-one feet of olive and bluish
grey, soft shales, through which are distributed a few thin flags. The shales
contain many fossils, and in some of the sandy layers casts of Gonidtites
Pattersoni are not infrequent.

The section thus far described is that exposed in the Snyder, Hartman and
Parrish gullies and the escarpment at the foot of Hatch hill. The measure-
ments for the remainder of the Portage strata were made in the Grimes gully.
The lowest rock exposed in this ravine is 375 feet above the base of
the Portage strata and is composed of flags or very thin, blue sandstones
separated by layers of shale, usually light-blue or olive, sometimes dark, and
occasionally black and bituminous.

Fossils, except plant remains, are exceedingly rare. A very large and
exceptionally fine specimen of Lepidodendron. Chemungense, fifteen feet in

length, now in the State Museum at Albany, was taken from one of these thin

‘'SSIdYN ‘ATIND SAWIYD ‘Wv4 GHIHL 34O dOL IY SSNOLSGNYS S39VLYOd

ENATIVH dOOMNAM

>

ee.
pS a She

NW SLW1d

LurHEr—Portacrt SANDSTONES. 93]

sandstones about ten feet above the bottom of the exposure, and a slab from
a layer of densely black slate immediately overlying the layer of sandstone,
had on one surface the impression of a number of fish scales and plates.

The general character of the material and of the stratification of the suc-
ceeding 135 feet of the section in this ravine is quite uniform, though the pro-
portion of sandstones varies at different horizons, with a gradual increase
toward the top. Fossils are rarely seen. Impressions or casts of Gondatites
Pattersoni occur occasionally on the lower surface of the sandstones, and large
forms of Spathiocaris Hmersoni are sometimes found.

Near the knife factory, im this ravine, a sandy layer four inches thick,
and forty feet above the Lepidodendron layer before mentioned, has on its
upper surface a very interesting bed of plant remains of lignitic character, in
which are hundreds of specimens, some of them several feet long. The
majority are not in a condition to be identified, but many fragments of
Lepidodendron oceur. The only traces of animal life so far observed in this
bed are two specimens of a large Orbiculoidea, species undetermined, and one
large Conularia. One hundred and two feet above the plant bed, a band of
sandstones two feet thick, forms the crest of a cascade sixty-seven feet high,
known as the “Second Falls.” The “ First Falls” are near the knife factory
and ‘are produced by the waters of a lateral ravine flowing over the side of
the main gully. They are about sixty feet high. Above the sandy layers at
the top of the second falls the shales and thin sandstones come in again and
continue a little more than sixty feet, to near the top of the “Third Falls.”

In the face of the precipice at the third falls, and exposed in the walls of
the canyon, a thin layer of soft blue sandy shale has been found to contain
Cardiola retrostriata, Pleurotomaria capillaria, Palwoneilo muta, Goniatites
Pattersoni and Bactrites, also a finely striated Cardiola, species undetermined ;
a distinctively Portage fauna. Twenty-four feet higher, and nine feet below
the top of the fall, occurs a layer of bluish sandstone, four inches thick, that
splits easily near the middle and discloses impressions and casts of a consider:
able number of fossils. The most abundant form here is apparently Liorhyn-
chus quadricostatus. Many of these are an inch in breadth, Smaller speci-
mens bear some resemblance to LZ. //mitards. A small form of cltrypa reticu-
laris is also abundant. An Orbicu/oidea, species undetermined, is common ;
Productella speciosa and Ambocelia wmbonata var. gregaria occur sparingly,

This fossiliferous layer has been traced for several rods along the vertical
sides of the ravine, but the most diligent search has failed to discover this

fauna or any other fossils in this horizon elsewhere in the Naples valley.

32 Revorr or He Svare GEo.oatst.

In the large ravine, six miles east of Grimes valley, near the Big Elm, in
the town of Italy, Yates county, loose fragments of a layer of the same
character were found from approximately the same horizon.

According to the measurements made, this layer is 599 feet higher in the
strata than the base of the Portage group, as previously assumed. ‘The fauna
contained in it is the lowest of a distinctively brachiopodous character that
has been discovered in this vicinity, and no recurrence of a fauna of Portage
characteristics has been observed above it. The sandstone layer at the brink
of the falls is one foot and four inches thick, compact and of a light blue color.
Above it there are exposed in this ravine forty feet of sandstones of the same
character, except that a few of the layers are schistose. They are from a few
inches to two feet and six inches thick, and are separated by thin layers of
very hard blue shales, These are the Portage sandstones. A solitary speci-
men of a large Atrypa reticularis is the only fossil yet observed at this horizon.
Aboye the sandstones, ten feet of soft, dark bituminous shales complete the
Grimes gully section. :

On the opposite side of the valley on the steep slope of Hatch hill, the
sandstones form a well defined and prominent terrace that shows the southern
dip of the strata very plainly.

In Caulkins’ gully and the quarry on the south bank, the sandstones are
yery compact and thicker, and the proportion of shale much less.

In the Tannery gully and Kaltenbach’s quarry, the section differs but
slightly from that in the Grimes gully, though some of the sandstones are more
inclined to a schistose condition. Their character is the same at the exposure
near the water works’ Reservoir.

In the rayines at the head of Italy hollow, eastward in Yates county, the
sandstones are well exposed, generally in thinner beds, and with an increasing
tendency to be schistose.

For nearly fifty feet above the sandstones, the section in the Naples valley
is composed principally of dark and black shales, in which the most diligent
search has failed to discover any fossils, and the few interstratified sandstones
are likewise barren.

Above this, the sandstones again predominate and are somewhat lighter
colored. The lowest fossiliferous layer observed above that at the third falls
in the Grimes gully, is on the road leading easterly across Deyo Basin, two
miles south of the village of Naples, a little south of the schoolhouse on the
road from Naples to Ingleside. This layer is exposed by the roadside near

the foot of the hill, five or six rods from the Ingleside road. Tt is an isolated

i)

| Atrypa reticularis
44 Streptorhynchus Chemungeuse

Amboccelia umbonata, var. gregaria

Aijing 3.4ox0H ¥

SauojSpuos UY} puD S2|OYUG

. 4 Dictyophyton tuberosum
4
[ar * | | Productella speciosa
hole =>
oy
we SF
oo
<a
oP v-— —
4? is) ====> Productella speciosa
Led ——— aes)
=5 89
25 4
i ———
ORES SS Dictyophyton tuberosum
200
=== =A {Spinter mesacostalis
4 — > Atrypa hystrix
fo) Seas | Productella speciosa
9 oS - || Amboccelia umbonata, var. gregara
= , Hystracanthus depressus
a \Crinoids sp. indet
is}
x
wo
4]
a3
Do
au
©
3=
DS Si=a
=
Qe
che
==
Sees;
a
SH
rau
2
uo
au
alg
5
ae
532
OSG
3 af
=¢
3 =a | Dictyophyton tuberosum
O< G ee ES eee
© A -
Qs 2;
35 5
=o =e Lelorhynchus quadricostat
= uadric
NS H EEA TAS ue
Productella speciosa
Amboceelia umbonata, var. gregaria
a i Orbiculoidea sp.
Leptostrophia mucronata

| Cardiola retrostriata _
Pleurotomaria capillaria

i Palzoneilo muta
Goniatites Pattersoni

| Cardiola sp.
Bactrites

THE Upper PortaGr AND Lower CHEMUNG ROCK SECTION AT THE SOUTH END
OF THE NAPLES VALLEY.

¥

LurHEer—Porrack SANDSTONES. 933

exposure and its stratigraphic position can not be ascertained with precision.
It is, however, not far from one hundred feet above the top of the third falls
sandstones. The layer is a compact sandstone, five inches thick, and contains
the following fossils :

Dictyophyton tuberosum,

Llystracanthus,

Spiriter mesacostalis,

Atrypa hystrix.

Productelli speciosa.

Ambocalia umbonata var. gregaria.

Crinoid stems and heads, sp. und.

This is clearly a Chemung fauna. About twenty feet higher in this
exposure a sandy layer contains Productella speciosa quite abundantly, and
forty-two feet above the lower fossiliferous layer there occurs a bed of plant
remains, In which J). tuberosum and two or three other species of fossil
sponges are common. Other Chemung fossils are also found here.

On the road leading from Naples village to West Hollow, near the resi-
dence of Charles 8. Sutton, one of the thin sandstones of this horizon exposed
at the roadside contains Orthis Tioga, Liorhynchus mesacostalis, Productella
spinulicosta, Ambocelia umbonata, Atrypa reticularis and sections of erinoid
columns.

In a layer in the west branch of the Tannery gully, opposite M. Hatch’s
house, Atrypa reticularis, Orthothetes Chemungensis, Ambocalia umbonata,
and a mass of crinoid plates and segments occur. This horizon is a little
higher than the others mentioned.

Above these fossiliferous layers, others occur at frequent intervals, in
which the number of individuals and of species, which nearly or quite all
belong to the ordinary lower Chemung fauna, is much increased, sometimes
producing more or less persistent calcareous layers. The sandstones also
become coarser and hghter colored.

From the foregoing it will be seen that the heavy sandstones at the top
of, and above the third falls in Grimes gully are the “ Portage sandstones,”
and are the upper and most southerly division of the Portage group. They
are here about fifty feet thick, including the interstratified shales, and from
599 to 650 feet above the bottom of the lower black band.

Toward the east from Naples, the line of outcrop of these sandstones is
easily followed around the head of Italy hollow, thence with a northerly bend

over Italy hill, and then south above Keuka lake, crossing the valley about

234 Report OF THE STATE GEOLOGIST.

two miles southwest from Hammondsport, and bending again to the north on
the east side of the lake. The deep valley of Seneca lake carries it far to the
southward again, but the condition of the sandstones, which have become
generally thinner and schistose, makes it more difficult to trace. It crosses the
valley, however, somewhere in the vicinity of Millport.

The wells of the Watkins Salt Co., at Salt Point, two miles from the head
of Seneca lake which, at the present date. are the most southerly ones
operated for the production of salt, were begun in the lower part of the Port-
age group; and the mouths of the wells of the Ithaca Salt Co., at the head of
Cayuga lake, are nearly in the horizon of the base of the Portage.

Westward from Naples, all parts of the group appear to increase in thick-
ness, the shales are generally softer, and the sandstones more compact and
heavier bedded. This is especially the case with the upper beds. They
are frequently exposed in the ravines on the sides of the valleys of
Honeoye and Canadice lakes, Springwater valley, and the valley south of
Conesus lake.

In the Stony Brook glen, two miles south of Dansville, the sandstones
appear at the top of the banks at the railroad bridge. . In a soft shale a few
feet below them, Cardiola retrostriata, Goniatites Pattersoni, and Aulopora
annectens are common.

The high ridge west of the Dansville valley carries the line of their out-
crop northward to about a mile south of Union Corners, where it bends to the
south and follows the west side of the Nunda valley to the south end, where it
is well exposed in Stone Quarry hill, three-quarters of a mile south of the village
of Nunda. Quarries have been operated here for many years in the layers of
compact samdstone, aggregating about forty feet, that are most accessible.
Apparently the full thickness of the formation is not exposed. The fossil
known as Sp/rophyton cauda-galli is common here. It does not occur in the
Naples section, but is very abundant in the sandy layers of the Portage in the
western part of the state, and is sometimes found in the middle portion of the
group, ucoides verticalis occurs here sparingly.

Underlying the heavy sandstones in the old quarry where the reservoir
of the Nunda waterworks is now located, there are five feet of bluish, blocky
shales in which are imbedded numerous small calcareous, and sometimes
pyritiferous concretions. (Goniatites Pattersoni and other Portage fossils occur
in the shales, but are very rare. This peculiar deposit is found over a large
area. It increases in thickness rapidly to the western border of Wyoming

county where it is about seventy-five feet thick.

LurHEer—Porracrk SAanpstones. 935

The exposure of the Portage sandstones in the walls of the deep gorge of
- the Genesee river, near the high bridge of the Erie railroad, is by far the most
extensive and best known. ‘The thickness of the individual layers and the
aggregate thickness of the sandstones appear to be greater here than elsewhere.
On the west side of the river, a short distance below the village of Portage
ville, a bed of sandstones, nearly all of which are compact, is separated by
six feet of shales from a similar bed about thirty-five feet thick, beneath
which the concretion bearing shales are exposed with a thickness of eight feet.
The upper bed of sandstones was extensively quarried during the construc-
tion of the Genesee Valley canal for material for locks, culverts and the great
aqueduct that crossed the river at this point.

Above Portageville the fall in the river is very slight, and the horizon of
the upper sandstones is above the river bed for several miles to the south.

The Genesee Blue Stone Co. has a large quarry in these upper beds,
about three miles south of Portageville, near the tracks of the Western New
York and Pennsylvania railroad, the product of which is used in Rochester
and New York city.

The next good exposure westward is in the gorge of Wolf creek, one-half
mile below the village of Castile. A band of black shales is exposed near
Hopkins & Son’s mill, and the sandstones are below it. The top of the
sandstones is here 150 to 200 feet lower than the crest of the ridge between
the Genesee river and the Silver lake basin, and the line of outcrops is carried
northward by the configuration of the land, and crosses the ridge about three
miles north of Castile. It bends southward around the Silver lake basin, and
again to the north over the high lands between the lake and the Oatka Creek
valley. }

The extensive quarries of the Warsaw Blue Stone Co., at Rock Glen,
expose about thirty-five feet of these sandstones, As a stratum of the conere-
tionary shale is exposed in the bottom of the quarry, it is probable that the
layers utilized are those of the middle and lower beds.

From the records of the salt wells in the southern part of the Warsaw
valley, it appears that the total thickness of the Portage rocks is here 800 to 850
feet, or about 200 feet greater than in the Naples section, thirty-five miles east.

The high plateau in the western part of Wyoming county, between the
Oatka Creek valley and the valley of Tonawanda creek is covered by drift,
and the bed rock is rarely exposed.

The large ravine near Varysburg presents a fine section of the shales of

the middle Portage that reaches the lower part of the sandstones, thereby

236 Report oF THE STATE GEOLOGIST.

furnishing a datum from which the location of the sandstones on the plateau
may be ascertaimed with a good degree of accuracy. At the south end of the
Tonawanda Creek valley and in the vicinity of North Java and Java Center
the sandstones are covered by drift.

In a deep ravine two and one-half miles north of Strykersville, cut
through the lower soft shales, some heavy layers of sandstone aggregating
fifteen to eighteen feet in thickness, occur at the top of a cascade known as
Johnson’s falls. They are very compact and present exactly the same
appearance as the upper beds.

The upper stratum, about eight feet thick, is exposed at Java village, in
the bed of the stream, where it crosses the main street. In the ravine above,
there appear first about twenty-five feet of black fissile shale, then seventy-five
feet of soft, blue shale, in which the small concretions abound; then sixty
feet of typical upper Portage flags and hard shales to the bottom of the upper
sandstone beds.

In the northern and western parts of the town of China, the rocks are
covered by drift; but in the southwestern part, near the village of Arcade,
in the Cattaraugus creek valley, the upper sandstones are exposed in a quarry
that has been operated for many years. The rock section is about twenty feet
thick. Some of the layers are very hard and compact, others are rather
schistose. These beds are quite barren, but on the road leading eastward
from the village, Chemung fossils are common at an horizon of fifty feet above
that of the quarry.

Westward from Arcade, the upper limit of the Portage group is found in
the high hills on the south side of the valley of Cattaraugus creek, with exten-
sions towards the south in the numerous lateral valleys.

There are probably some thin outliers of Chemung rocks of small area
on the north side of the valley in Erie county.

The upper Portage flags and sandstones are exposed along W alnut creek,
in Arkwright, and in the bed of Canadaway creek, at and above Laona, where
one compact layer, four feet thick, and another three feet thick that splits
easily into flags, are quarried. The compact layer is also quarried near
Brockton, and in the village of Westfield. It disappears beneath the waters
of Lake Erie, about three and one-half miles southwest from Westfield.

The Portage sandstones, so well defined in Livingston and Wyoming
counties, in their westward extent gradually lose their heavy bedded character,
and in the vicinity of Lake Erie they are composed mainly of thin sandstones.

separated by thin layers of hard shales.

GeoLtocic Map
eee OF THES.
‘Townsurp OF NAPLES

Ontario County NY.

D.D.LUTHER,

iC
SOG) Oe
3) O

“Ay

LEGEND
eae, |
esse)

CHEMUNG

PORTAGE

GENESEE

\

SS

Canandaiqua

Lake yj
y
—

\\

Pall
Cy

Ss
=
o
ay
g

2

o

y
\

oe
ZAIN

(>
WY

Mii

LZ
Kill

KS
er

¥

S \
jie, |
y Zprmym att

MANN

\

ALIN

AS

lai Wf

) adi Ss
Hit as FN ND
Ce & 7a eae al INT TORN rapp Hil
e ne

WYNKOOP, HALLENBECK,CRAWFORD CO. NEW YORK & ALBANY.

>

GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

THE ECONOMIC GEOLOGY OF ONONDAGA COUNTY, NEW YORK.

JAMES HALL, DANA bU TEER:

State ¢ reologist. | Assistant.

1895.

7
4
=

pata. ints

Herewith I ‘submit. my report on the Economic Eieolony of

eounty, New York, | or ee :

_ Respectfully yours,
D. DANA LUTHER.

f

\

¥

River Point

y,

es

Eni pase . N : Fi
‘wha, es J
s\ Maj ys .
Wills Gy

Zs
Gi

syn
Ua ri's + A ells
we

Xi
N

\ \
SS

7
5.)

y

teas

NE
i" li WZ,
pK

<
0\\
©
nn’

ni
nN

\)
1

A

y
'

”

\'
'

Ww.
Ss
F
Al)

VV A4nyse
La

iY

AA N\

&

papeie TM
MY
/ \ \
AN wif ty (

Keg OT

ee

MAP OF ONONDAGA COUNTY.

The Economic Geology of Onondaga County, New York.

By D. Dana Luruer.

CONTENTS.

Locarton, AREA AND TopoGRAPHy, p. 241.

THE GEOLOGIC SUCCESSION, p. 246.

Clinton Shales, p. 247. Niagara Limestone, Outcrops, p. 247; Quarries, p. 248; Product, p. 249.

Salina Group, Red Shales, p. 250; Distribution, p. 250; Use in Manufacture of Brick, p. 251; Salt,
p. 251; History of Manufacture and Product on State Reservation, p. 251; Borings for Rock Salt,
p. 253; Tully Wells, p. 254; Solvay Co., Product and Handling of Brine, p. 256; Ammonia-soda
Process, p. 257; Well Records, p. 268. Gypseous Shales, p. 264; Lithologic Character, p, 264;
Gypsum, Occurrence, p. 265; History of Production, p. 266; Product and Producers, p. 266.

Lower Helderberg Group, p. 267: Water-lime, p. 268; Geologic Relations and Distribution, p. 268;
Mode of Exploitation and Manufacture, p. 269; Producers and Product, p. 270; Stromatopora Bed,
p. 272; Blue Limestone, p. 272; Edifices of, p. 272; Product of Quick-lime, p. 272; Producers of Lime-
stone, p. 273.

Oriskany Sandstone, Character, Thickness and Extent, p. 274.

Upper Helderberg Group: Corniferous Limestone, p. 275; Distribution and Characters, p. 276;
Economic Importance, p. 277; Mode of Quarrying, p: 277; Producers and Product, p. 278; Archi-
tectural Examples, p. 279.

Hamilton Group: Marcellus Shales, p. 279; Goniatite Limestone, Extent and Use, p. 279. Lfamil-
tow Shales and Sandstones, Geologic Character and Distribution, p. 281; Agricultural Importance,
p. 281; Other Economic Uses, p. 282. Tully Limestone, Character, Extent, Quarries, p. 282.

Chemung Group: Genesee Slate, Distribution, p. 284. Portage Shales and Flags, Character, Distri-
bution, Fossils, p. 285.

Quaternary Formations, p. 286; Drift, p. 286; Buried Valleys, p. 286; Gravel, p. 287; Sand,
p. 287; Product and Producers, p. 287; Clays, p. 288; Distribution, Product and Producers, p. 288;
Brick, Manufacture and Product, p. 288; Analysis, p. 290; Marl, Extent, p. 290; Portland Cement,
p. 291; Mode of Manufacture and Product, p. 291.

Oondition of the Rock Strata, ;. 292; Dip, p. 292; Folds, p. 293; Faults, p. 293; Anticlines and
Synclines, p. 293; Eruptives, p. 294; Gas, p. 297.

TABLES OF Economic Propucts, p. 298.

Location, Area And Topoarapny.

The county of Onondaga is, in shape, a nearly rectangular parallelogram,
lying between 42° 45’ and 43° 15° north latitude, and 0° 29’ and 1° 6’
longitude east from Washington. It is bounded on the north by Oswego
county, the Oneida river forming a part of the boundary line at the north and
Oneida lake on the northeast; on the east by Madison county, Chittenango
creek making a part of the county line; on the south by Cortland and
Cayuga counties, from the latter of which it is separated in the southwest
corner by Skaneateles lake, and on the west by Cayuga county. The greatest
length of the county from north to south is thirty-three miles, the average
length being twenty-nine miles and the average width twenty-eight mies. It
has an area of 812 square miles, or 519,680 acres, of which 459,229 acres are
Jand, the remaining 60,451 acres representing the combined area of the lakes.

16 241

2492 Report or toe Srare GERoLoacist.

In the northeastern part, a section five or six miles wide, parallel to the
shore of Oneida lake, is low and flat and, in the town of Cicero, embraces
several large swamps. The northern parts of the towns of Manlius, Dewitt
and Clay lie partly in this tract which, on the eastern borders of the county,
extends as far south as the Erie canal, and includes the territory about the
foot of Onondaga lake and its outlet. The average altitude is not greater
than 390 feet A. T.

In the town of Lysander the land is gently undulating in the eastern
part, but higher in the western part where the rounded drift hills sometimes
rise 100 to 150 feet above the level of Cross lake and the Seneca river. The
northern part of the town of Van Buren is rolling, the sides of the hills fre-
quently showing the soft red and green shales of which they are composed.

The Erie canal crosses the county a little north of the center, at an
elevation of 401 to 409 feet A. T. The territory lying north of the canal is
generally flat or gently undulating. The soft Clinton, Niagara and Salina
shales that here constitute the bed rock, offer little resistance to denuding or
disintegrating forces, and are buried under drift or, when exposed, smoothly
rounded over.

The southern part of Van Buren and the northern parts of Elbridge and
Camillus are generally flat and low. The broad swampy intervales of Nine
Mile creek, Carpenter’s brook and other streams, extend through the higher
and rougher southern parts of Camillus and Elbridge to the line of the
Auburn branch of the New York Central railroad.

South of this lower and comparatively level part of the county, a succes-
sion of rugged ledges and vertical walls of limestone, constituting the Helderberg
escarpment, stretches across the county, on a very irregular, but nearly east
and west line. This escarpment is the upturned edge of the limestones of the
Salina, Lower Helderberg and Corniferous groups, lying upon each other to
the thickness of 400 to 500 feet. It causes an abrupt elevation of the surface
to the height of 800 to 850 feet A. T. From the top of the escarpment to
the south line of the county the average elevation gradually increases to 1,500
or 1,600 feet A. T., and the extreme height reaches 2,020 feet A. T., at the top
of South mountain, in the town of Fabius, and 1,968 feet, at Ripley hill in
Spafford. This high land in the southern tier of towns forms the summit
ridge or watershed between the drainage areas of lake Ontario and the Sus-
quehanna river.

The waters of Limestone creek, Butternut creek, Onondaga creek, Spat.

ford creek and Skaneateles lake flow toward the north and reach the sea by

Luraer—Economic GroLocy or ONONDAGA County. 943

way of Oswego river, lake Ontario and the St. Lawrence river, while Fabius
creek, which has its rise in a small spring on the top of Pompey hill, together
with Labrador brook, the outlet of the Tully lakes, and Cold creek in Spafford,
flow south into the Tioughnioga river, and reach the ocean by way of the
Susquehanna river and Chesapeake bay.

Five deep, narrow valleys extend from the south line of the county in a
northerly direction and break through the Helderberg escarpment at different
points. These principal valleys, named in order from the east, are: Limestone
creek valley, Butternut creek valley, Onondaga valley, Otisco or Nine Mile
creek valley, and the Skaneateles lake valley. They have many lateral
branches, some of them quite extensive, and deep rocky ravines with high
cascades are numerous.

Limestone creek valley is situated near the east line of the county. The
DeRuyter storage reservoir for the Erie canal at the southeast corner of the
county, is near the south end of the valley. From the reservoir, which is
about 1,250 feet A. T., to Delphi the descent is rapid, and a deep gorge has
been cut by the stream through an immense mass of glacial drift that chokes
the valley at this point. From Delphi to near Manlius the descent is slight ;
the sides are sloping and there is an intervale half a mile wide. At Manlius,
where. the valley is cut through the limestone, it is narrower and rocky.
Edward’s falls, one and one-half miles south of the village, are ninety feet
high, and below them is a narrow gorge with high banks. Just below the
village of Manhius the valley of the west branch of Limestone creek is connected
with the main one by a deep ravine, one-half mile long, ending at Brickyard
falls, seventy feet high. Above the falls the valley, which is generally rough
and irregular, extends towards the south for several miles. Pratt’s falls, five
niles south of Manlius, in this valley, are 137 feet high. Below the junction
of the two streams the valley spreads out rapidly. The floor is somewhat
uneven, and the bed rock is but thinly covered, cropping out in many places.
The sides of the valley are rough and steep, with bare masses and clifts of
limestone, 200 to 300 feet high, on both sides as far as Fayetteville. North of
Fayetteville the bordering hills are lower and do not extend beyond the
Erie canal.

Butternut creek valley is connected at its head in the western part of
Fabius with the valley of Limestone creek by a wide, high, east and west
valley, and also with the Tully lake plateau by an extension which has a
southwesterly course, with the drainage in the same direction. Near Apulia,
where the bottom of the valley is highest, it is 1,225 feet A. T. It is narrow

244 Report oF THE Stare GEOLOGIST.

and rocky for most of the distance to Jamesville, the average descent being
about fifty feet per mile. North of Jamesville, where it breaks through the
limestone beds, it becomes a narrow gorge, with a cascade at Dunlop’s mills,
where the first saw mill in the county was built, in 1792, and the first grist
mill, in 17938, by Asa Danforth. Half a mile north of Dunlop’s mills the
“Jamesville cut,” a canyon fifty rods wide, 250 feet deep, and three miles
long, diverges towards the west and connects Butternut creek valley with the
Onondaga valley. The Delaware, Lackawanna and Western railroad runs
through this cut and the entire length of the Butternut creek valley south
of Jamesville.

The Onondaga valley is the north end of an ancient river bed that, at the

=

S

close of the glacial epoch, had been filled with drift to so great a height in
What is now the township of Tully, that a col was formed at an elevation of
1,200 feet A. T., the water on the south side following the old channel to the
Susquehanna river, and on the north to Onondaga lake and the Seneca river.
At the point where the southern boundary line of Onondaga county crosses,
the valley is about three miles wide, the southern extension of Butternut
creek valley coming into it just there from the east and nearly doubling the
width. The sides are 300 to 500 feet high and very precipitous. The col,
or separating ridge, lies on the north side of all the Tully lakes, except Crooked
lake. Two and one-half miles north of the county line, the high upper section
ends abruptly, and the floor of the valley sinks, in the distance of about half
a mile, from 1,200 feet A. 'T. to 800 feet A. T. At the foot of this declivity
a well sunk near the middle of the valley, which is here about a mile wide,
penetrated 400 feet of clay, sand and fine gravel, and was abandoned without
reaching bed rock, from which it appears that the morainic filling of the old
channel is at least 800 feet thick. Many copious springs burst out on the
steep slope-of the gravel bed, forming small streams that unite with the Vesper
brook which comes in from the west through a deep ravine, and over a cascade
seventy feet high, and together make the Onondaga creek. The water of these
springs is saturated with lime taken up from the drift. and large iasses of
travertine have been deposited in many places. An extensive deposit of red
clay, the material of which is evidently derived principally from the red Salina
shales, lies nearly across the extreme south end of this lower section of the
valley. From this point to Syracuse, about seventeen miles, the valley is
from one to two miles wide, the sides of the bordering hills sloping gently at
the base, but becoming precipitous and in many places rocky in the middle

portion, while the upper part is a succession of rounded eminences that rise

‘ "ATINL SO NMOL SHL NI STISM L1¥S
S,ANVWdINOD SS300%d AVAIOS SHL SO Y/OAYSSSY SHL WOYS ‘W33YD VOVONONO 3O ASTIVA SHL SO GNZ HLNOS BHI JO MAlA

QS COI MYO YOASNSTAVH'dOOWNAM

I aLWid

Lururtr—Economic Gronocy or OnonpaGa Counry. 945

500 to 800 feet above the bottom of the valley. The intervale is an alluvial
plain having an average descent toward the north of twelve feet to the mile.
Unlike the other four valleys that have been excavated through the Helder-
berg escarpment in this county, the Onondaga valley becomes wider after it
reaches the hard limestones in the vicinity of the Indian reservation, about
midway between the head and Onondaga lake, spreading out into a plain one
and one-half to two and one-half miles wide. The sides of the valley decrease
somewhat in height, but are still 250 to 400 feet high, steep and rocky,
abounding in cliffs and ledges, the location of many quarries. The ridge on
the east side of the valley extends to Ley creek, a little north of the head of
Onondaga lake, with a deep valley crossing it, two miles from the north end,
through which the Erie canal and the New York Central railroad find passage
to the eastward into the city of Syracuse. On the opposite side the hills recede
toward the west, and do not reach quite so far north. The basin of Onondaga
lake is located in the low section of the county, extending in a northwesterly

direction from the line of the Helderberg escarpment. It is excavated to the

2
depth of 450 to 500 feet in the Salina red shales, and is a continuation of the
old channel, which is now the valley of Onondaga creek. The bottom of this
channel at the head of the lake has been found to be fifty-two feet below the
levelvof the sea. At the Solway Co.’s first well at Tully, the drill penetrated
400 feet of sand and clay without reaching the rock, and in two wells on the
east side of the valley, forty-five feet of drift was found in one, and in the
other, 590 feet therefrom toward the center of the valley, 322 feet. The

latter well is about 2,000 feet from the center of the valley. Nowhere in the

. middle of the valley is bed rock exposed, nor has it been reached by drilling,

and there is every probability that the great depth of the old channel below
the bottom of the present valley, found at both the head and the foot of this
lake, is continuous throughout its whole length.

The Otisco lake valley has its beginning in Cortland county, and extends
in a northwesterly direction. From the foot of Otisco lake southward it is
about half a mile wide, with steep sides, where the soft shales are frequently
exposed. The hills adjacent to this part of the valley rise from 800 to 1,000
feet above the bottom of the valley. The valley is narrower north of the
lake, and the outlet, known as Nine Mile creek, runs among drift hills and
shale knolls to Marcellus village, where a narrow rocky canyon begins, which
is cut through the Helderberg escarpment to the depth of 250 feet, about four
miles to Marcellus station. From this point Nine Mile creek flows toward the

northeast through a narrow valley having steep sides and a flat alluvial inter-

246 Reporr or tHe Stare GEOLOGIS?.

vale that has a very slight descent. One-half mile south of Marcellus a wide,
deep opening has been cut through the east side of the Nine Mile creek valley
down to the top of the limestone. This is the head of the Cedarvale valley,
which extends in a southeasterly direction and joins the Onondaga valley
near South Onondaga.

The Skaneateles lake valley, near the western border of the county, has
a general direction from the southeast to the northwest. Skaneateles lake,
which is sixteen and one-half miles long and has an average width of about
one mile, occupies the southern part of the valley. About the head of the
lake the sides are precipitous and rocky to the height of 100 to 400 feet, then
they slope gently upward to the height of 700 to 1,100 feet above the level of
the lake, which has an elevation of 860 feet A. T. Toward the north end of
the lake the width of the valley is greater, the hills are much lower, and the
gentle slope of the sides is continued qnite to the shores. The passage
through the limestone escarpment is about one-half mile wide and three miles
long. The rocks are abundantly exposed, but there are no high clitts nor
deep rock cuts. North of the New York Central railroad the valley winds
among low hills of drift or shale in a northerly direction across the town of

Elbridge to the Seneca river.

Tur Geonocre Succession.

The rocks exposed on the surface in this county are all of sedimentary
origin, with the exception of a small amount of eruptive matter in a single
locality. The geological formations to which they belong, named in order
from the lowest, are:

, Clinton Group.

INTE, Raul Go50050 5 G0Go none ooee Le
| Niagara Group.
> ~ .
Salinas Beriodmerme aac creer eee | Red Shales.
| Gypseous Shales.
Lower Helderberg Period ............ Hydraulic Limestone.
Outen, Ttawslooobuns oonbance ode Oriskany Sandstone.
Upper Helderberg Period............ Corniferous Limestone.
Marcellus Shales.
laleyoollivoyay IRGC a odoongbodoaconaas - Hamilton Shales.
Tully Limestone.
(Chemunoar eniodan rere terete j Genesee Slate.

| Portage Group.
\ Glacial Drift.

Quaternary System 4
| Champlain Deposits.

1 000'AT.

S5O0AT

—s

EE =
SEZ —SEEEEZEZA
ZZ

EE

ase
AE SLD
LEILA A
EIDE
Pompey

Figure 1. THE NORTH AND SOUTH ROCK SECTION THROUGH ONONDAGA COUNTY,

LurHEr—Economic GroLogy or OnonpaGa Counry. Y47

Clinton Shales.

The lowest sedimentary rock formation exposed in this county is the
Clinton shales of the Niagara period. These are the bed rock underlying the
north part of the towns of Cicero, Clay and Lysander. This territory has
an average elevation of perhaps a little below 400 feet A. T. The surface
is gently undulating and the soil is generally sandy or gravelly. The streams
are all very sluggish and do not usually cut down to the rocks; hence
exposures are very rare.

In the vicinity of the village of Brewerton, at the foot of Oneida lake,
the covering of drift is quite thin, and the rock is frequently uncovered by
the grading of the highways and in digging cellars. The rock is nearly all a
soft olive green shale, quite light colored when first exposed but, owing to
the iron it contains, it rapidly becomes a dark rusty brown. Some thin layers
occur, composed largely of fine grains of iron. They oxidize rapidly on
exposure and crumble into dust.

The Disciples church, in the village of Brewerton, stands on a knoll about
ten feet high, composed of the Clinton shales, which are exposed near the
sidewalk in front. Forty or fifty rods south from the station of the Ontario
and Western railroad, the highway cuts through a similar knoll, exposing four
or five-feet of the shales, and other similar small exposures occur toward the
east along the shores of Oneida lake, and toward the west near the Oneida
river, though they are not sufficiently dispersed, nor of such a character as to
permit the accurate measurement of the thickness of that part of the Clinton
group included in the surface rocks of this County.

. The exposures at Brewerton are fifteen to twenty feet above the Oneida
river, and three miles from the line of the outcrop of Niagara limestone, and
the elevation is very nearly the same, so that the thickness of the intervening
beds of shale can only be determined by ascertaining the amount of dip, which
can not be done by direct measurement on account of the lack of good expo-
sures. It is impossible, for the same reason, to locate the contact line between

the Clinton and the overlying Niagara shale.

Niagara Limestone.
The limestones of the Niagara period are exposed at several places along
a line from the northwest corner of the county to Bridgeport, across a section
of country which has an elevation of 375 feet at the east line of the county,

and rarely rises above 400 feet A. T., except in the northwestern part of the

?

town of Lysander. Their position is sometimes indicated by a low ridge, but

248 REPORT OF THE Srare GEOLOGIST.

this ridge is nowhere high enough to affect the drainage to any appreciable
extent, except as it forms the northern rim of a shallow basin from eight to
ten square miles in extent, known as the Cicero swamp.

Diedrich’s quarry, from whicli Niagara limestone has, for many years,
been taken for building purposes and for the manufacture of quicklime, is
located in the western part of the village of Lysander, a few rods south of the
crossing of the Main street and the little stream known as Ox creek, which
ruus through a shallow north and south valley, about thirty-five rods wide at
this point. The rock is exposed or very thinly covered for the entire width of
the depression and on both banks for a short distance. A small quarry for-
merly existed on the east bank, a few rods north of the street, and another a
mile further north, near Baird’s corners, from which a considerable amount of
building stone was taken. A kiln for making quicklime was located there.

At Diedrich’s quarry the stratum uncovered is about five feet thick and
consists of a number of layers fron, two to six inches thick, of very hard, fine
grained, dark grey bituminous magnesian limestone. Some of the layers are
quite even in thickness, while others are mere lenticular concretionary masses
and are very uneven. Thin scaly seams of black bituminous matter separate
the layers. Small irregular cavities, lined with crystals of calcite are common.
Fossils are very rare. The quarries mentioned have supphed the principal
part of the cellar and foundation stone used in the village of Lysander and
vicinity, and slabs of considerable size have been used for the covering of road
culverts and like purposes. A fair quality of quicklime was formerly made
here, and the ruins of the old kiln remam. The rock breaks easily across the
bedding with a straight smooth face and makes a handsome wall. Under the
chisel it has a shghtly conchoidal or cuppy fracture. The thickness of the
Niagara limestone at this locality is unknown. It was penetrated eleven feet
in a well dug near the residence of O. O. Brown, forty rods northeast of
Diedrich’s quarry, and the bottom was not reached.

On lands owned by Otis Bigelow, Esq., two and one-half miles northwest
from Baldwinsville, the limestone is covered by three to four feet of drift over
several acres. Workings, known as Ham’s quarry, were formerly operated at
this place. The stone used in building Houghtaling & Bigelow’s large
flouring mill in Baldwinsville was quarried here, and it has been used exten-
sively for cellar and foundation stone, bridge abutments, culverts, and similar
work in the vicinity. It was also used in the construction of the Delaware,
Lackawanna and Western railroad. The stratum of limestone is about four-

feet thick in several layers, some of which are quite even in thickness.

Lururr—Economic Gronoay or OnonpaGca Counry. 249

Apparently the upper parts of the limestone beds have been removed, and
the layers remaining are those of the base of the strata.as dark bluish shales
appear in the bottom of the quarry. The excavations extend over a consider-
able area, but are very shallow. They are now partially filled with. water,
and are overgrown with weeds and bushes, thus precluding satisfactory
examination. The line of outcrop crosses the Seneca river, one mile north
of Newbridge. No outcrop is now visible, but loose slabs are very abundant,
and were used in the construction of the Oswego canal, which occupies a part
of the old river bed.

On Peter Young’s farm, one-half mile northeast from Cigarville (Clay
corners), in the town of Clay,.the limestone has been uncovered by the
removal of one to two feet of soil, and about 500 cubic yards of material for
culverts and bridge abutments were quarried from the stratum, two feet thick,
of good stone found here, and used in the construction of the Syracuse
Northern railroad. A smaller amount was hauled to Brewerton for cellar
stone. One layer, eight inches ‘thick, is compact and quite even; the rest is
not so good. The quarry has not been worked recently. The ground here
is nearly level, and the old pit is now partly filled with water, and no outcroy
is visible.

In the town of Cicero, two and one-half miles east of the village of
Cicero, the limestone lies very near the surface of an area more than one hun-
dred acres in extent, and blocks of it, formerly scattered over the fields, now
make a large part of the fencing for a number of farms. A quarry has been
in operation for many years, on land owned by Mr. O. Whitney, and has
‘supplied the principal part of the building stone used in this vicinity. About
three feet of hard, compact limestone in fairly even layers, three to twelve
inches thick, are here exposed. The color of the rock is very dark, dull
grey, and where it has been long exposed in the farm fences, it is
black. Some parts are very finely granular in character. Cavities of irregular
shapes, lined with crystals of calcite are quite abundant. Quicklime was
formerly made in a kiln situated about one-fourth of a mile east of Whitney's
quarry,

At Bridgeport, the limestone is exposed in the bed of Chittenango creek,
where it appears as a bar and creates a water power of considerable value.
Although the Niagara limestone is but a few feet thick, the ease with which
it can be quarried, and the position of its line of outcrop across the northern
tier of towns, makes it of considerable economic value to that part of the

county. No other building stone except, in some localities, a few erratic

250 Report OF THE STATE GEOLOGIST.

boulders, can be obtained without the expense of transportation for fifteen to
twenty miles.

At present the output from the five quarries, which have been opened in
it, is not large, but the amount is governed entirely by the demand for good

building stone.
g

Salina Group.

The Salina group is composed of two thick deposits, which differ greatly
both in appearance and character. The lower beds are known as the Red
shales, and the upper as the Gypseous shales.

Red Shales. The Red shales include many layers of green shales, and
clouded or mottled red and green beds are of frequent occurrence. The red
color is, however, very pronounced, a strong brick red; the green is a light
but generally distinct pea green. Some of the upper layers near the contact
line are olive. Red is the predominating color in the lower beds, and green
toward the top. The shale is very soft and clayey, crumbling into dust on
exposure, if dry, or turning to clay, if wet. Some of the green and olive
layers are fissile to a slight degree.

In the Onondaga Brick Co.’s quarry, near Warner's, there occurs a layer
of coarse sandstone that resembles the Medina sandstone. Thin layers of
drab magnesian limestone occur among the shales in all parts of the sub-
group, but more abundantly toward the top. The Red shales constitute the
bed rock in a belt averaging about seven miles wide, extending across the
county parallel with the line of the Erie canal, which may be taken as its
southern boundary. From this territory there are to be deducted outliers of
the succeeding Grypseous shales in the hills in the northern part of Camillus,
and the northeastern part of Syracuse.

In the town of Van Buren, and particularly in its northern part in the
vicinity of Dead creek and the Seneca river, the hills are beautifully banded
and clouded in green and red where the shales come to the surface, or are but
thinly covered by clay produced by their disintegration. The range of hills
north of the West Shore railroad, near Warner's station, is mainly composed
of shales of the middle and upper parts of this sub-division. The Onondaga
Vitrified Brick Co. takes the raw material for its very large output of brick
and tile from one of these hills, where a section seventy-five feet thick 1s
exposed, The Central City Brick Co. also has a quarry in nearly the same
horizon, in a low hill one and one-half miles southeast from Kirkville, near the

Erie canal, from which it manufactures brick extensively.

LutHEerR—Economic Gronocy or OnonpaGa County. 251

The state ditch across the peninsula in the southwestern part of the town
of Lysander, formed by the loop of the Seneca river near Jack’s Riffs, was
excavated through a bed of quite hard olive and green shales and thin lime.
stones, reaching the top of the Red shales. An exposure of banded green
and red shales occurs on the east side of Onondaga lake, not far from the cor-
poration line of Syracuse, and the redder shales may be seen farther north
toward Liverpool. Neither salt nor gypsum is found in any considerable
quantity in the Red shales. Their only economic value lies in the fact that
they supply an inexhaustible quantity of good material for the manufacture
of brick. For this purpose the shale is dried and screened to remove any
fragments of limestone or sandstone, then pulverized, after which it is brought
to the proper consistency by the addition of water and pressed into the form
of bricks. The bricks are dried and baked in immense conical kilns till
thoroughly hardened.

The Onondaga Vitrified Brick Co. manufacture 10,000,000 building
bricks annually. The Central City Brick Co. produced, in 1895, at their new
plant at Kirkville, 1,500,000 ornamental pressed brick and expect the annual
output to be many times that number hereafter.

At the top of the Red shales, thin layers of drab limestones, some of them
cellular, and all cracked and seamed and containing the hopper shaped forms
which indicate the former presence of salt crystals, make up a large part
of the rock strata, the remainder being composed of soft, clayey, olive, or
harder, bluish and drab gypsiferous shales. Some of the olive layers show
even more plainly than the limestone, that salt in seams and veins and crystals
was once abundant in these rocks, and the disturbed condition of the strata
makes the supposition not unreasonable that one or more layers of rock salt
have been removed by dissolution. The great deposits of rock salt in the
western and central New York salt fields are all in this horizon, as is the bed
reached in the wells of the Solvay Process Co. at Tully, which is, beyond
doubt, the source whence has been derived the enormous quantity of salt held
in solution in the brines of the Onondaga lake basin, from which there has
been manufactured without material diminution of the strength of the brine,
ten million tons of salt, equal to a bed of rock salt ten feet thick, covering
310 acres.

Historical Epitome of the Salt Industry. The first salt manufactured
from the Onondaga Salt springs was on the sixteenth day of August, 1653,
by Father LeMoyne, a Jesuit missionary, who says: ‘“ We tasted the water of
a spring, which the Indians were afraid to drink, saying it was inhabited by

252 REporT OF THE Strate GHOLOGIST.

a demon who renders it foul. I found it to be a fountain of salt water, from
which we made a little salt, as natural as from the sea.” The Onondaga
Indians continued to own and control the salt sprigs until 1788. During the
intervening time they had learned to use it with their food and to manu-
facture it. Small quantities of it were transported to Quebec and sold by
them, and samples were carried by traders to Albany.

On the twelfth day of September, 1788, by the treaty of Fort Schuyler,
under which the Onondaga Indians ceded to the State of New York all their
lands, it is declared that “the salt lake and the lands for one mile around the
same, shall forever remain for the common benefit of the people of the State
of New York and of the Onondagos and their posterity, for the purpose
of making salt, and shall not be granted, nor in any wise disposed of for
other purposes.”

In the month of May in that year, Comfort Tyler, with the assistance
of an Indian who guided him to, and pointed out the salt spring, made thirteen
bushels of salt in nine hours, with a fifteen-gallon iron kettle. In the winter
ot 1789-90, Nathaniel Loomis made between 500 and 600 bushels, which he
sold for one dollar per bushel. In 1791 or 92, Wm. Van Vleck and Jeremiah
Gould “made salt in chaldron kettles set in arches.” In 1793, the first
“block,” four caldron kettles set in one arch, was erected by Moses Dewitt
and Wm. Van Vleck. In 1798, the Federal Company erected a plant, contain-
ing thirty-two kettles in blocks of four each.

By act of Legislature, in 1797, the state assumed direct control of the salt
reservation, and on June 20th of that year, William Stevens was appointed

Superintendent of the Onondaga Salt Springs. Since that date the annual

reports of the Superintendent show the amount of salt made each year. In
1798, it was 59,928 bushels) In 1862, it was 9,053,874 bushels, the largest
amount made in one year. In 1810, the water of Yellow brook was used to
dnve a water wheel] to elevate the brine, and pumps, driven by horse power,
came into use about the same time. -

About 1521, the manufacture of coarse salt by solar evaporation was
begun. In this process the brine is exposed to the sun’s rays in large shallow

wooden vats until crystallization takes place. At the present time about

seventy-five per cent. of the salt produced at the Onondaga Springs salt
reservation is made by solar evaporation. The first wells were dug at the
edge of the marsh at Salina. One of them, the first of any note, was sunk by

Superintendent Kirkpatrick, about 1806. It was twenty feet square and —

thirty feet deep. In 1820, Major Benajah Byington was authorized to bore

—~S «

LuTHER

Economic GroLocy or OnonpaGa Country. 253

for rock*salt anywhere on the reservation. His explorations were made in
the higher land east of Salina. They resulted in failure. In 1825, Simon
Ford, engineer in charge of the salt works, drove a tube, twelve feet in diam-
eter and made of staves thirty-two feet long, to a depth of thirty feet, and
then removed the mud and earth from the inside, thus making a new well.
In 1826, a well was sunk at Liverpool, that appears to have been in the shales.
It was the only well that did not require to be curbed. In 1827, wells wer
sunk at Geddes, Salina, and one mile north of Salina. In 1830, iron tubes,
twelve inches in diameter and three and one-half feet long, were clamped
together and sunk, by boring, to a depth of sixty feet. In 1831, the Onondaga
Salt Co. bored a well, 160 feet deep, to good brine. In 1839, a well was sunk
at Salina by the state to the depth of 600 feet, in search of the bed of rock
salt that was thought might be in the immediate vicinity and supply the
saline qualities to the waters of the marsh, by contact with subterranean
streams. No crystals of salt were found. It had been ascertained that the
strength of the brine was greater as the depth from which it was taken
through the tubular wells on the borders of the lake and marsh was increased.
At sixty feet it was twenty-five per cent. stronger than in the old shallow
wells. By the use of tubes constructed of iron or of hard maple wood
banded: and clamped with iron, wells were sunk in the mud and sand of the
low lands about the head and east side of the lake, which reached the depth
of 225 to 340 feet in the Syracuse wells, 150 to 310 feet at Salina, and 80 to
100 feet at Liverpool.

In 1851, a well was sunk in the middle of the valley, at the head of the
lake, to the depth of 414 feet, through the following strata :

smtnCeaMUEeACNSaAMG: 60. ec ciaw em ce eee ene wee. 34 feet.
iiieeremieiotimcolored Clay fos... 2... ee eee 148°“
SEIS: BEPC. aye Se aie a DQ sc
SES GE 1 A oe Boe
Joe DESH ICL 6 Sed RONDA Ses a enor iP
STIS 20 2a 1 2 Og i
LER GIN? cg is Sd aU MS acs en ore!
DEIR ROL GLASS 3.5 ERIN Roo Hit Saks

Except as to the thickness of the layers, this appears to represent the
section in all of the producing wells, the best brine being found in the clear
gravel, which is reached at varying depths in all of the wells. In 1888, fifty
wells were in operation, and produced all of the brine from which salt was

manufactured on the reservation. They were in five groups, as follows:

954 Report oF THE Stare GEOLOGIST.

“Syracuse” group, fourteen wells; “De Wolf” group, six wells; “Gere”
group, six wells; “Salina” or Marsh” group, twelve wells, and the “Geddes”
group, twelve wells, and produced brine of an average strength of seventy
degrees salometer.

In 1878, the truth of the long maintained assertion of Professors Eaton,
Hall, Vanuxem and other geologists, that beds of rock salt occur somewhere
in the rocks of the Salina period, was proven by the discovery at Wyoming,
Wyoming county, N. Y., in a deep well sunk for oil or gas, of a bed of rock
salt, seventy feet thick, 497 feet below the top of the Corniferous limestone,
and at the base of the Gypseous shales. The Onondaga Salt Co. had sunk a
well 715 feet at Liverpool, in 1867, after which no deep wells were put down
im Onondaga county, until 1881, when the Solvay Process Co. drilled 1,040
feet at Jamesville in the Butternut Creek valley, seven miles in a southeasterly
direction from Onondaga lake, having reached the red shales at 587 feet,
without finding salt. In 1882, the Solvay Co. put down a well at Cedarvale
(formerly called Montfredy’s mills), about eight miles southwest from the
head of Onondaga lake. The mouth of this well was about 700 feet A. T.,
and not far from the horizon of the top of the Corniferous limestone. Red
shales are reported to have been reached at 705 feet. Brine was found, but
no rock salt. The total depth of this well was 1,157 feet. About this time
a deep well was sunk at Danforth, two and one-half miles south of the lake,
in the Onondaga valley. No record of this well is obtainable.

In 1884, Thomas Gale, Esq., had a well bored about three miles northwest
of Syracuse, on the north side of Onondaga lake. The surface elevation at
this well is 435 feet A. T. According to Dr. Englehardt’s record, the Niagara
limestone was reached at 527 feet. Brine was found at 485 feet, 532 feet,
1,895 feet and 1,500 feet, but no rock salt. In the same year the state well,
situated on the south bank of the new channel of Onondaga creek, 1,000 feet
east of the lake, and which had already been sunk to the depth of 430 feet,
ending in red shale, was drilled to the depth of 1,969 feet. The mouth of the
well is 369 feet A. T. Niagara limestone was at 578 feet. No salt was found,
nor brine, except a small quantity in the upper shales. The sinking of these
two wells settled the question as to the presence of rock salt beneath the
reservation; but the search was resumed toward the south, in the Onondaga
valley, by the Solvay Process Co.

In 1888, a well was begun in the town of Tully, eighteen miles south of
Onondaga lake, in the middle of the south end of Onondaga creek, near a
cross road at the foot of the drift hills. It was abandoned after penetrating

09.04QS MT YD 1078N SD WHOBAMAY

a

Lurner—Economic Grotocy or OnonpaGa Counry. 255

400 feet of gravel and quicksand, without reaching the bed rock. Another well
was immediately started, 1,400 feet east of the latter, and on the side of the
valley in the Hamilton shales. The Corniferous limestone was reached at 718
feet, and rock salt 498 feet lower, the distance between the top of the Corni-
ferous limestone and the top of the rock salt being one foot more than in the
Pioneer well at Wyoming. Drilling ceased after forty-five feet of salt had
been penetrated. No red shales were found. The total depth of this well,
which is known as the “Tully well,” is 1,261 feet. The elevation of the
mouth of the well is 901 feet A. T. The next well was put down one mile
south of the village of Cardiff, three miles north of the Tully well. The top
of the Corniferous limestone was reached at 244 feet; then 500 feet of lime-
stone and 100 feet of red shale were drilled through without finding
rock salt.

In 1889, ten wells were drilled by this company along the foot of the hill
on the east side of the valley, north of the Tully well. Nine of these wells
stopped at or near the bottom of a bed of salt, forty-one to forty-seven feet
thick. One of them passed through this bed, forty-three feet, then through
twenty-five feet of shale, reaching a second bed of rock salt, fifty-four feet
thick. Below this bed, forty-one feet of “ Magnesian shale” and ten feet of
gypseous shale were penetrated.

In 1890, ten wells were sunk. The records kept by the drillers show that
in one of them 318 feet, and in another 220 feet of rock salt were penetrated,
but the number of beds and the thickness of intervening beds of shale, if any
such were found, is not recorded.

In 1891, eight wells were drilled to the salt beds. In one of these, four beds
were found, respectively forty-six, seventy-four, thirty-six and sixty feet thick,

making a total of 214 feet of rock salt; these were separated by three beds
of shale, forty, thirty and thirty feet thick.

In 1892, another well was sunk on the east side of the valley, making
thirty wells in all. On account of its inconvenient location the “Tully well”
has not been utilized. The twenty wells sunk in 1889 and 1890 were located
in five groups, each group consisting of four wells, one at each corner of a
rectangle, 400 feet long, from north to south, and 150 feet wide. The groups
were 1,000 feet apart, and very nearly on a north and south line, making the
distance between the wells at the north and south end of the series 6,000 feet.

Of the nine wells drilled in 1891 and 1892, five were added to the groups
as then arranged, two were located further south and formed a new group,

and two made a new group north of the others. The seven groups were

|

256 Report oF ‘THE STare GEOLOGIST.

designated A, B,C, D; I, FG, beginning at the south. Very careful records
of the strata, penetrated im drilling the wells, were kept by Mr. Hugh Graham,
who superintended the work. The records of wells No. 1 and 4 of group
“A,” No. 1 of group “B,” and No. 1 of group “C” are especially minute in
detail. From them the diagram on page 263 has been compiled.

The land on which the wells are situated, has an upward slope from the
bottom of the valley, becoming steeper very rapidly, and a few rods east of
the wells the Hamilton shales crop out all along the hillside. The thickness
of the drift passed through varies from eleven feet in two of the wells nearest
the hill, to 256 feet and 322 feet m two of the most westerly, or nearest the
nuddle of the valley.

In the fall of 1895, the Solvay Process Co, began the work of sinking ten
wells on the opposite side of the valley, about three-fourths of a mile west of
group “A.” The wells are located im and about the mouth of the Vesper
ravine. The record of the first well, completed on the west side, known as

“No. 30.” 1s as follows:

Surface clevationt. eee cee... ee eee 833.2 feet ALE.
Top of Corniferous limestone at............. Giore
Salt ats... 2S See eee eee diag bye

Measurement by Locke level shows the mouth of this well to be 497 feet
below the base of the Tully limestone, as exposed near the road leading from
Tully to Vesper, the outcrop being one-quarter of a mile south of the well.
Allowing ten feet for dip of strata, would give 483 feet + 675 feet — 1,158
feet for the thickness of the Hamilton and Marcellus shales at this point:
Salt was reached 499 feet below the top of the Corniferous limestone,

The record of well “No. 32” is:

Divit*. oe 2 ee 12 feet
Corniferous. limestone at... 2. 20. 0s. 645 “ 75 feet thick.
Oriskany sandstone at .:/..../25... 120") “Ei &
Salt atliec switch, | ee ee es ere LteOS So) Oras 7
Depth otavelly 25) ..2 operas iets fe fe

Well “No. 33:
Corniferous limestone at... 2 ees eee 654 feet.
Rock salt*at et. 222.4220. 4 ee eee 1,164

The object sought by the Solvay Process Co. in drilling these forty
wells, was a sufficient supply of salt to be used at the company’s works
at Geddes, in the manufacture of soda-ash. The salt is dissolved out of the

bed and conveyed to the works by gravity, advantage having been taken of

s Uot| Vu OH

i
j=)
5
ra)
Oem
a To
wb ——_—— JF
oa oo
Ss 2D El| et Same
SSS es
tae Soh ASS
=20: ees oe andstone|
25 eee ve Heck
= ———
s ===> =— Gray
me sans = Lime stone
Q —
8 Se Bee black.
[a=) —— ia
> en
2 ——— = Gray
130 Er Magnesian
=| Limestone
== =
—— === Gray
=> Gypseous
oO === Shale
z z Greenish
3 45 Limestone
eS G Black
seous
2 Gypsee
Salt
cae
Shale

Ficure 2. THE ROCK SECTION IN THE SALT WELLS
aT TULLY; FROM THE SURFACE TO THE TOP OF
THE SALT aS IN WELt No. 1, Group B;
FROM THE TOP OF THE SALT TO BOT-

TOM As IN WELL No, 4, Group A, *

ae bec
a _
ven bedded
Limestone

Maqnesian

Marlyte
Soft

breccia

Corniferous

— Ath

GEE Stromatopora

26S Layer

' — aT
(4. = Wipes
Sa

=i

ee
°

S

ea Soo a

Se

@o

(ab,

© .

mM

aa

o y
a ZZ,

10, SS S= Gypsum

Lime ston¢
Ficuxe 3.—Tue rock-seetron ar P. C. Cor-
' ‘ sha aS
RIGAN'S QUARRIES AT SKANEATELES Fiaurer 4. SEcTION IN THE HEARD GYPSUM BEDS,
FALLS, ON THE SKANEATELES ONE MILE SOUTH OF LyNDON, N. Y.

OUTLET,

ai een ae EI OY,
Corniferous 1 _ ___ Limestone
pene
Soa
ee 2 ee ee ee
Oriskany s ; = Sandstone
pas

= SS Limestone

4ABmMmo 7

pe Sale
OSS
a8 IRS Stromatopora
DISS Bed

GuequapjeyH

~LLLL Neter
a ty jj jj j een

” Blue

ap == Limestone

yyy
LA ImesTone

ZZ Li,

=
Limestone

Prcure 5. Tne ROCK SECTION IN A. E, ALvorp’s
QUARRY, MANIIvS,

—Groy

Corniferouis
— Limestone

ES
616" PEG DSF tromatopora
Layer

yu Blue

Limestone

2s) fff %, mestorne
= Blue

32 Limestone

YY y Moers

Saequepjsy 4aanoq

= Blue

=F |_imestone

Ficure 6, ‘Tue ROCK SECTION IN THE BRITTON
AND CLARK QUARRY, NEA BRIGHTON,

Corniferous Ly Gray

1210" 4g Limestone

>...

= Limestone

wie Impure

Limestone

Suequepjey 4ASmMOo7T

SY Limestone

Ficure 7, Tue RocK SECTION IN THE SOLVAY
Process COMPANY'S QUARRY, AT Sprit Rock,

Luruer—Economic GroLoGy oF Ononpaca County.

to
Sl
|

the natural situation. The wells, having a surface elevation of from 720 feet
to 909 feet A. T., are from 319 to 508 feet above the Erie canal, 401 feet
A. T., which is, approximately, the elevation of the works.

About two miles southwest from the wells is Crooked lake, the only one
of the Tully lakes that has a northern outlet; this has an elevation of 1,198
feet A. T., or 284 feet higher than the mouth of the highest well. A dam and
gateway were built at the foot of the lake to regulate the discharge, and a
conduit of twelve-inch cast iron water-pipe was laid, through which the water
flows to the wells, where it reaches the salt bed through three-inch iron pipes,
placed inside of the six-inch well casings and, dissolving as much salt as it can
carry, becomes saturated brine. The pressure in the three-inch pipe forces
the brine up through the space between the two pipes to the surface, where
it overflows and is conducted to the twelve-inch cast-iron brine pipe, through
which it flows by gravity to the reservoir at Solvay.

Mr. F. R. Hazard, Treasurer of the Solvay Process Co., has kindly fur-
nished the following description of the Solvay process of manufacturing soda-
ash or carbonate of soda:

“Tn considering the ammonia-soda process, it 1s convenient to start from
two different raw materials, and to follow them through the several opera-
tions until they actually come together. For this purpose we consider salt
and limestone.

“Starting first, then, with salt. This is found in the condition of rock
salt at Tully, and is reached by boring wells in the familar manner. Fresh
water is introduced into the wells, where it dissolves the salt, and is forced to
the surface in the form of a saturated brine. The brine is then forced from
Tully to the works at Solvay, and enters the storage reservoir. From the
reservoir it is drawn as required into the works. On entering the works, the
brine first meets the waste gases from all of the operations, and is used to
wash them free of the last traces of ammonia. The ammoniated brine is then
allowed to settle a sufficient length of time for the deposition of the impurities
thrown out of solution by this preliminary process.

“Turning now to the limestone. This is quarried from the ledges at the
Split Rock quarries, and is broken to suitable sizes and transported in the
overhead cable tramway system, and finally delivered at the top of the lime-
kilns at the works. With the proper proportion of coke, the limestone is fed
continuously into the top of the kilns. When burned, it produces ordinary
quicklime, which is drawn from the bottom of the kilns. This is then placed
in proper vessels, where it is slaked with water, and stirred up into a milk of

Lg

258 Report oF THE STATE GEOLOGIST.

lime. This milk of lime is sent to the distilling vessels in the works, where it
meets the chloride of ammonia, produced in a later process. The reaction
which here takes place, converts the calcium oxide of the milk of lime into
‘alcium chloride, and sets free the ammonia which was held by the chlorine.

“In the burning of the limestone in the kilns, carbonic acid gas is produced.
This is pumped by suitable pumping engines, and after being washed in
water, is forced into the carbonating system, where it meets the brine which
has been previously supplied with the proper amount of ammonia. The
whole ammonia-soda: process depends upon the reaction which now takes
place. The carbonic acid gas first takes the ammonia and produces a carbonate
of ammonia. In the presence of this substance, and the excess of carbenic
acid gas, a double decomposition takes place. The carbonate of ammonia
takes the chlorine from the salt, and the sodium from the salt takes the ecar-
bonic acid from the’ carbonate of ammonia. By these reactions, two new
substances are produced, 7. ¢. chloride of ammonia and bicarbonate of soda.
The first of these is a liquid and the second a solid. By means of suitable
filters, the liquid is separated from the solid, and the solid bicarbonate of soda
is roasted in proper furnaces, driving off the excess of moisture, ammonia and
carbonic acid gas, and reducing it to the form of mono-carbonate of soda,
which is the ordinary soda-ash of commerce. After the necessary grinding
and screening, the product of the furnaces is ready for packing

“The chloride of ammonia in the liquid form is now returned to the distil-
ling columns, where it meets the milk of lime produced at the lime kilns, and
gives up its chlorine to the lime, thereby releasing the ammonia, which in the
form of gas is put back again into the process.

“ The chemical reactions of the ammonia-soda process are extremely simple,
and together form an almost complete cycle of operations. It only remains
to separate the chlorine from the calcium in the waste product, to make the
process absolutely perfect. Upon this point, many of the most able chemists
of the world are at present engaged. Although the chemical reactions are
without complications, the handling of the carbonic acid gas and the ammonia
present many practical difficulties, which it has cost many years of patient
study and experiment to overcome. The apparatus necessary for the proper
carrying out of the process has become complicated out of all proportion to
the apparent simplicity of the reactions. This, however, is to be accounted
for by the fact that the reagents to be handled are largely in a gaseous state.

“The ammonia-soda process differs radically from the LeBlane process,

which was its predecessor, in that the old process works largely in the dry

Lururr—Economic GroLtoagy or OnonpaGca Counry. 259

way, while the more recent process works entirely in the wet way to the point
of the production of crude bicarbonate of soda. As this can only be decom-
posed by heat, it is necessary to use, for this purpose, a single furnace opera-
tion. Fifteen years ago, probably about four-fifths of all the soda produced in
the world, was produced by the LeBlanc process. To-day it is safe to say
that the ammonia-soda process produces fully three-fourths of the soda-ash
produced in the entire world, and the remaining twenty-five per cent. alone is
produced by the LeBlanc process.”

The Solvay Process Co. was organized in 1881, for the purpose of
engaging in the manufacture of soda-ash, and other soda salts by the ammonia
process, under the American patents of Messrs. Solvay & Co., of Belgium, of
which it has exclusive control. Works were erected near the Erie canal and
New York Central railroad, a little west of the village of Geddes.

The following statement recently published is claimed to be authentic:

Capacity of works, 500 tons finished product daily. Present daily output,
350 tons finished product. Men employed, 3,000. Coal consumed, 1,000 tons
per day. Limestone consumed, 1,200 tons per day. Brine consumed, 800,000
gals. per day. Water, 30,000,000 gals. per day. Land occupied, 2,000 acres.

The “Mineral Industry” for 1896 (Statistical Supplement of the
Engineering and Mining Journal, Vol. IV, pp. 57, 58), gives in greater detail
the present amount and valuation of this company’s product, as follows:

“ A few more or less unsuccessful efforts were made before 1884 to make
soda in the United States, but the birth of the industry here must be said to
have commenced practically in 1884 with the manufacture of 11,000 metric
tons of soda-ash by the Solvay Process Company, at Syracuse, N. Y. This
Company was organized in September, 1882, with a capital of $300,000, and
commenced the erection of works with an estimated capacity of 30 tons of
soda-ash a day, and in 1884 it commenced regular production. To-day its plant
covers an investment of some $6,000,000, and has a capacity of 75,000 tons of
soda-ash alone at Syracuse. The improvements introduced from the very begin-
ning increased the output beyond the estimated capacity when the works were
planned, as is shown in the accompanying table of materials used and products
turned out each year. This valuable table contributed to the Mineral Indus-
try by the courtesy of the company, is in itself almost a history of the alkali
indystry. of the United States, for it covers probably nearly ninety per cent. of
the entire output. In 1894 and 1895, when there were a number of other
producers, the Solvay Process Company made about three-quarters of the

entire output and is now building a large plant near Detroit, Mich.

00 OF 00's
GZ Se 0016
20 ~ } rare?
a ce 9% | O0S"re
id 9) |
Pats Tos ybeeeae®
= |
= |
i ssa" (yep sieie'='<
S)
ra |
(ds) |
= . ES
“4 =e =
MT
2 |
= 0099 | 066
3 “BV ROOOIG
a GSS S68 ‘TOT
i 001 | ogg*rat
mS }
jae 00 1% 00066
"AOL ‘SNOT,
“688T

|

|
|
00 zr | sre |
00 ¢¢ | oer |
GB 9% | ~OOL‘OS
|
00.99 | 086
cL § 000'TT
st z | 000.06 |
GT 000001
ZL 1% | 00006 |
“MORI ‘SNOL
|
"S881 |

l j l
eee } ee tee eS Me MAI es avis a | meee | ewsccce
|
| |
=-=e | wereee weiwieg). jl tne ws ewe [i clasts ) cecces
i cp 2 Me eS (eee BAL to
Ps ths os Jace | nese Bre oo
0G 8% | OOL'ES 00 Z8 | 000K 00 ¢& ~~ 000‘ST
|
|
ee SA Rsk Ie oes en ane Ba Boeri er aay
00 99 | OKO 00 89 | ST9 00 OL 02S
| |
GL 000'8 tose Aer cone Weer tie ee
|
et | o00'%9 |00c | 000'%r | 00% | 00006
| | |
oI 000'09 | SG I o0u.2b | S&T 000'62
|
GZ 1$ | 000'8¢ - | co 1$ | 000’SF | Gz 14 | 00082
| | |
oo LE a sl my ay er
| |
‘m0INd | ‘SNOJ, “MOM T ‘SNOT, “aod ‘SNOL
|
“LS8T “9881 | “GR8T

00 OF

‘MOM

— 000°TT

_ 000°%%
-000'T%

000502

sort coro stes sss oqeipsYy BUIWN[S JO opixe,

Nien Sago pos om ies (OS *®D) wg ToT

Bpos jo oyeqdpug
speyship

o1ysne,)

SCOR AES ASOT FOO CSS Ro 5 300r %eae ‘Wse-epog
BO SS 3 OS TS ORO ae peonpoad rey,

eo ae SRN Spa de se 3 cs -ageqdyus ‘ermoululy

2 SPONPOLT

opIzneg

plow onmydyng

Pad OSG IS. SIO R50 oyeqdyns se viuouumy

ouojsoully]
oulIq 8B 4[BS

I :pasn $)pi.va) Dy

260

‘KN ‘ASNOVUAS

CSNOZ OLA NI)

‘SMMOM SSHOOUd AVATOS WHE AO SLONdOUd UNV ‘Ad CAWASNOD STVINALVA

Luruer—Economic Gro.oGy oF OnonpaGa Counry.

rans lig ee 99 | OOL | 00 99 oe ee sesso | | teens lp es ie |e tone teeess sees =-oapi pA BULB JO OPIXO
00 &6 OOL EO Le be (RCO), wy SAA Re Pe hee eeeee | omic Dare Neen A al A ST ee aN tae lee age rama cr oe CUED S (FOS %)) ao[py wMory
00 TL | OSE 00 TL OUS ears esr OOL CE Will eC, 8 | wstee- | eens | ceeees | BR en o5 crete e) egg are ocd ao upos Jo oyeydpng
00 OF =| O&b QO RO Fa POS a i | pis ese ys Se a a ee Vue na Sra clang At eee | MCR ICI | an brent 4 ate MEE emai aot speyshig
00.9% | 006 ~—»-00. 98-006 00 LE | 0F6'8 00 6g | 00r8 | 00 68 | ozs‘9 ODEOR, 080%) erent rons onsen Groene an” OIE MOG IED Ta
00 1F =| C0098 00 £4 | 090'08 00 99 | 00L‘3S 00 69 | 008‘S% 00 69 | 096°FI 00 09 | OBLTIT | Beer iat Galan ae Afar ash 2 hen o1gsney
00 £5 | 000‘OST | 0S 8% | OO9‘FOT | 00 Bg | 000°GR 09 €& | 0008 | 02 0 | 066‘0L Rey eie | OLeic0y Walaa. | cas os Ree ee MSG “Ust-epog
00.8 | O&b 008 | SIF 008 | OZ OORE OLGaeh hae Neroarpegidl esata? aba paces rect one oae poonpoad wey,
00 $9 SéI 09 S9 | SET 00 &9 =| OST CNATISYS) lhe yay Vanna Wells trite Baal | eee le ae aetier | ta a aan Raia oyeydins BrmouluLy
| | oy SJON PONT
cian? lO paceman ren ME 09T erica | epg Gi is 2d RODS DIO Seulietehes Se AIS Aa ICO ONS es ONIN IIIS fh bo C9 |
OO L OO See ||, mesancis OOF Se ase grec ee nl es RIESE all ROC RCO Sie sriee Sg | R I AAD eiaad eee poe otunyding
00 99 008"T 00 79 =| 06L'T 00 G9 | 009'T 00 OL | OLO'T 00 OL | OOP T OOS OO Mn OGG hip estas sasas cae a ait oyeyd[ns sv vrmourary
02 € — | 000¢e 0g € | 000'0% 0g § 063‘LT 0G § G8L‘8I 0S § OPE ‘LT 0c & O89 FT es leeeecu erste SoC de eine it wae ee Gb Cire)
86 & | 000002 «GB % 0000LT | 83 GeBF‘ZOL | 66% OST‘S2T | 93% | OIGZIT | GZ & (OY steht oa (co a tear tet ake ie pouinsuod [B0,)
00 T 000022 | 00 T 000‘0FG | 00 T 0L0‘661 00 T OF8‘60G | 00 T 008‘68T | 00 T ORTAEGT) | Ria as ee eae canned ee OOS O ULL,
0) 1% 000‘sTZ | 00 1% | oo0'z6t | 00 1% | O00‘091 | 00 TH | O00‘OST | 00 TH | 900 cE | 00 TH | OOO'GTE |---~ 7-777 *+* outa 8B 418g
| | | | ! pasn sppriwopv yy
: | -. | Ie |
| | . |
“dO ‘SNO], | ‘Horug ‘SNOT, | ‘HOINd ‘SNOT, | “MON *SNO J, "Old ‘SNOT, | “MOI “SNOT,
“G681 “V68T S681 | C681 1681 “0681

ORLA Np)

‘XN “ASOOVUAS ‘SHNOM SSHOOUd AVATOS AHL AO SLONGOUd ANV ‘AU GAWOASNOOD S'IVIAULVA

“ ( “SNOT,

262 Report oF THE State GEOLOGIST.

Lardner Vanuxem, in his report on the Geology of the Third District
of New York, 1842, describes the “shales and calcareous slates,” in which, it
now appears the salt beds occur, as the “second deposit” of the Onondaga
salt group. He does not state the thickness of the strata included under that
designation, nor can any be definitely given now, as it is exceedingly
variable. Along the line of outcrop the thickness is not more than fifty
feet, perhaps considerably less in some places, while at Tully, including the
salt, it 1s more than 300 feet.

The layers of rock salt are also very unevenly bedded, as is shown by the
Tully salt well records, and are probably largely heterogenous in character,
as in the Livonia, Retsof, Lehigh and Greigsville salt mines in western New
York. Mr. Graham states that the contact rock over the upper bed of salt in
the Tully wells is limestone.

The following table is copied from the Solvay Process Co.’s record.
Nearly all of the wells end at the bottom of the upper layer of salt :

"LLIMSG ‘'AYYVNO XOOTIM ‘SGS8 WNSdAD SHL NI SSAVD

Ai 3LW1d

LurHer—Economic Grotocy or Ononpaca Counry. 263

|
|
|

& : fe Z | : | | | | TOTAI

5 Wee mh S| | 3 = 4 «|: SALT.

fee) 498 | 45 pore rash en | | 45

eT eee Hie 2| 481 | 44 | 40 | 74| 30 | 36 |-30 | 60 | 214
pra| 404 | 45 | 32 | 57 | 58 | 50 | 42 | 28 | 180

eho Gin Gace lit 318

i} 2| 765 | 30

Bit: aca | 3 528 | | | 225
0d | 4). | 25) 29

5 | 520 | 54) 54

Mere). 518 | mal Oe Ae

aoe) 600. | 47 | | ar

[| -9 497% | 45 | 5

C ...—E f oe | 46 | ie
eis 4 5O7 | 44 44

Bee 544 | 43 | 25 | 34 97

yy! eva: J 2] 547 |48 ‘
fi 8 |» 548 | 48 | 48

mea) 545+ | 50 | 50

Mie. 558 | 45 | 45

2 10a ee ao | 44

ee Ore es | 543 | 41 | 41
4| 556 | 39 39

5 | 551 | 35 | 35

teal. 546. | 35 | 35

| SR ae 4%

Pe ert eer |. 3 542 | 40 | 40
| 4} 539 | 41 41

fee 638 | 38 | 38

ah Sane | EEE Res -
| 3 530 | 38 38

264 Reporr or THE Stare GEOLOGIST.

The third division of the Onondaga group, designated by Vanuxem
the “Gypseous deposit,” is locally known under the name of the “ Gypseous
shales.” It is the surface rock over a belt having an average width of two and
one-half to three miles, parallel with the foot of the “ Helderberg escarpment,”
with long extensions toward the south where the Limestone, Butternut,
Onondaga, Marcellus and Skaneateles creeks have broken through and worn
away the’ heavy limestones of the Corniferous and Lower Helderberg forma-
tions and uncovered the gypsum beds.

The contact line with the second deposit, that is, with the horizon of the
salt beds along the north side of this belt, lies mostly in the low alluvial
plains previously mentioned, and not far from the course of the Ene
canal.

The contact lme with the hydraulic limestones of the Lower Helderberg
group in the south, is usually found at varying heights in the face of the
Helderberg escarpment. The territory embraced between these lines is much
of it broken and hilly, and the rocks are abundantly exposed throughout
nearly its whole extent, though the exposures are not usually continuous for
a very long distance.

The “Gypseous deposit” is composed in part of beds of fine grained
magnesian or dolomitic limestones, generally in thin layers, sometimes so
finely laminated as to become a slaty, calcareous shale. It also contains thick
masses of gypsum and soft gypsiferous shale in two courses, separated by a
bed of limestone forty or fifty feet thick. In the thicker and more compact
layers of limestone, freshly broken blocks show the rock to be very dark,
almost black, in the interior; but after exposure the color changes to an ashen
grey or medium dark drab, sometimes showing a slight pink shade. It 1s very
like hydraulic limestone in appearance, but the proportion of clayey admixture
is so large as to injure or destroy its cohesive qualities. In the middle and
lower beds it is frequently more or less porous or cellular. The cavities are
sometimes an inch or more in diameter, very irregular and ragged in shape,
and lined with a fine brown dust. When of this character, they are very
unevenly distributed through the rock and most frequently are found on the
surface of a layer, or opening into a joint.

In other layers, the cavities are found to be much more numerous, occu-
pying in the aggregate nearly half the space of the rock, and having the form
of circular cells, with the diameter ranging from one-fourth of an inch down
to a needle point. Usually the cells in a particular layer of limestone have a

considerable degree of uniformity in shape and size, but occasionally -the con-

‘LLIM3Q 'AYYVNO SONWUBASS ‘SGA WNSdAD Ni S3AVD

A 31W1d

Lururr—Economic Gronoagy or Onondaga County. 2

trary is the case. They are smaller in the lower beds. These cellular lime-
stones are the “ vermicular limestones ” of the older reports.

In the shaft sunk to the rock salt beds at Livonia, N. Y., at the depth of
1,356 feet, thirteen feet above the salt bed, a stratum of this cellular magne-
sian limestone was reached, in which the cells were filled with salt. A large
block was placed in a running brook, and in a few hours the salt had been
dissolved out, leaving the rock in precisely the same condition that it presents
when found in loose fragments or in the outcrops in this county. In the
beds of limestone lying between the principal gypsum deposits, and more
abundantly in that underlying the lower gypsum beds, hopper-shaped mud
casts of what are supposed to have been salt crystals, are numerous. They
are found in both the cellular and non-cellular layers.

The “needle cavities,” or stylolites, are found in all the limestones,
but more abundantly in the more compact layers at the top of the deposit.
Gypsum occurs in layers, veins and nodules throughout the entire deposit,
but most sparingly in the upper limestones, where it is either anhydrous or
in the form of selenite. The two layers of gypseous shales, in which occur
the gypsum beds that are quarried, appear, wherever this horizon is exposed,
clear across the county, the upper bed forty to sixty-five feet thick, the lower
twenty to thirty feet thick; the proportion of clayey matter being much
greater at some localities than at others. The upper bed is better in quality,
more convenient of access and much thicker. Most of the plaster quarries
now operated are in it. It appears to have been deposited in quiet waters,
the deposit consisting of gypsum and clayey matter, the sulphate of lime
greatly predominating at some horizons, while in others the proportion
was small, and a stratum of shale was formed. Where the bed has been
exposed for a length of time, it looks like a bank of soft dark shale. The
lines of deposition are very even except where water has penetrated to it
through a crevice in rocks above and dissolved out the gypsum, leaving a
cavern partly filled with the shaly residuum and fallen fragments of the
overlying limestones. These caverns or “pockets” are quite common and
sometimes extensive. Where the bed of overlying limestones is thin, it is
broken through to the surface and “sinks” are formed, thereby increasing
the inflowing stream of water and the rate of dissolution.

In the Heard quarry, a number of these partially filled cavities are
exposed, extending from the bottom of the workings to the top, fifty to sixty
feet. Many of the minor disturbances of strata in the vicinity of the outcrop

of the gypsum beds are doubtless due to dissolution in this manner.

bo
(oP)
or)

Report OF THE STaTE GEOLOGIST.

There are abundant evidences, too, of crystallization after deposition. In
the richer parts of the beds lenticular layers of clear white or transparent
crystalline gypsum, an inch or two in thickness, occur, and the laminae above
are arched in conformity with them. They may be seen by the side of the
Split Rock road, a mile west of the “ House of the Good Shepherd,” and in
nearly every plaster quarry. The rock of this lower bed is sometimes called
“black plaster,” as it is much darker colored, and this affects its commercial
value, though the actual difference in purity is said to be slight.

The gypsum beds are exposed in many places in the vicinity of Fayette-
ville, in the town of Manlius, and south of Lyndon, in the town of Dewitt ;
also near Brighton, in Onondaga, and in the southern part of Geddes. They
are also exposed along both banks of Nine Mile creek, and on the line of the
Auburn branch of the New York Central railroad in Camillus.

The first discovery of sulphate of lime or gypsum in the State of New
York, was made in 1792, by William Lyndsay, on Lot No. 90, in the town of
Camillus. In 1808, a stock company was organized and began the business of
quarrying and exporting gypsum, or land plaster, an industry that for many
years was second only to the manufacture of salt in its importance to Onon-
daga county. It has declined somewhat in late years, but recently discovered
processes of making prepared wall plaster, into which gypsum enters largely,
as the “ Adamant,” “ Eureka” and “ Paragon,” promise to increase the demand
for it.

When the gypsum is to be used as land plaster, it is quarried by the
ordinary methods used in soft rock, then broken with sledges into pieces con-
venient for handling, and hauled to the mill in carts. It is then broken in
stone-crushers or crackers, and ground fine by the use of mill stones. It is
then ready for use. For the manufacture of wall plaster it is calcined, becom-
ing, when pulverized, plaster-of-paris.

The principal men or firms who quarry and grind plaster, are: Thos.
W. Sheedy, who has a mill at Fayetteville, and a quarry east of Fayetteville.
He also buys rock plaster. Output, 2,000 tons annually. Bangs & Gaynor,
Fayetteville, buy most of their stock from quarries in vicinity. Output, 5,000
tons. Lansing & Son, Dewitt, quarry two miles west of Fayetteville, mill on
the bank of the Erie canal. Output, 2,000 tons. F. M. Severance & Co.,
Dewitt, quarry at the “Heard” beds, two miles west of Fayetteville.
Output 4,000 tons of rock plaster, shipped by canal out of county.
tobert Dunlop, mill one-half mile north of Jamesville, quarry one and

one-half miles northeast from mill; grinds and sells 2,000 tons annually.

'SNIINVIN ‘AYYVNO S.GQYOMIY NI asa VYHYOdOLVINOYLS SHI

LurHer—Economic GroLocy or OnonpaGa County. 267

E. B. Alvord & Co., Jamesville, buy and grind 2,000 tons. A. E. Alvord,
Syracuse, buys and grinds 3,500 tons.

There are a number of small quarries in Manlius and Dewitt, besides
these mentioned, but their product is sold to the mill owners and dealers, and
the output is included in the amount stated.

Mr. A. E. Alvord opened a quarry near Brighton, two and one-half miles
south of Syracuse, but is not operating it at present. None of the quarries in
Camillus are now worked. IL. D. Sherman, at Marcellus falls, grinds about
300 tons annually; quarries near the Marcellus station.

So far as known, the bed of gypsum quarried by F. M. Severance on the
Heard farm is the thickest in the county, measuring sixty-five feet including
some thin intercalated beds of shale. A few feet of dolomitic limestones at
the top of the Salina group have very obscure lines of deposition, but split
easily into thin slabs with a somewhat conchoidal fracture. These are pro-
fusely scattered over the surface of the ground in the regions of the outcrop
of this horizon, and are utilized as material for farm fences, etc. The needle
cavities are very common in them, but fossils, except Leperditia alta, are
wanting, or at least very rare.

Lower Helderberg Group.

The hydraulic limestone beds of Onondaga county, provisionally referred
to the Lower Helderberg group, are composed almost entirely of even
courses of very dark blue, fine-grained limestones, from one to five feet thick.
Exposure changes the color to a medium light, dull, bluish grey, and makes
the lines of bedding very distinct. With two or three exceptions, all of

the beds are composed mainly of calcic carbonate and contain but a small

- amount of magnesian, or clayey matter, as compared with the “Magnesian

deposit” below. They are known as the blue lime beds, and from them
almost the entire output of quicklime of the region is taken. A few courses
contain too much impurity for use in the manufacture of quicklime, and are

utilized as building stone. The rock splits easily along the lines of depo-

sition, and breaks across them with a straight, even fracture. In some
localities, masses of Stromatopora occur, and the rock loses its regular strue-
ture. The two beds of hydraulic limestone which give the name to this
group, lie near the top of it, separated from each other by one to four feet of
impure, blue limestone. The upper layer is a little more than four feet
thick at the eastern boundary of the county, becoming thinner till it pinches

out entirely in the Split Rock quarries, but reappearing near Marcellus falls

268 Report or THE SrarE GEOLoGIsT.

in Watkins’ quarry, where it is two feet, ten inches thick, and attaining a
thickness of four feet, two inches in Corrigan’s quarry at Skaneateles falls,
near the western line of the county. Here it is separated from the lower
bed by a shaly parting of only a few inches, the whole making practically
one bed, nine feet, six inches thick.

At Manlius, the beds are separated by four feet, two inches of blue lime-
stone; at Street’s quarry, near Onondaga hill, by one foot, eight inches; at
Marcellus falls, by one foot, seven inches, and at Skaneateles, the beds prac-
tically come together. The lower stratum of water-lime at Jas. Beahan’s
quarry, in Manlius, is four feet, one inch thick; KE. B. Alvord’s quarry, in
Jamesville, four feet, five inches; at Britton and Clark’s, near Brighton in
the Onondaga valley, five feet, two inches; at Walker’s quarry, near Mar-
cellus falls, it is five feet, three inches; and at Corrigan’s, at Skaneateles
falls, the part of. the bed that appears to be this stratum is five feet,
one inch thick. At Split Rock, the upper bed is well exposed and measures
vwo feet, two inches thick at the southeastern part of the quarry. It is
separated from the Onondaga limestone above by only a thin nodular shaly
parting, which here represents the Oriskany sandstone. It thins out and
entirely disappears in the western part of the quarry. The place of the
lower stratum of water-lime is here occupied by a bed of blue limestone
nine feet, one inch thick. But twenty-one feet, eight inches below the upper
layer, there occurs a layer one foot, five inches thick that is hydraulic
limestone, though of an inferior quality. It was not observed elsewhere.
This hydraulic limestone is brittle, clinking, compact, fine and even grained,
dark colored, sometimes black in the interior, but, when exposed, quickly
becoming a dull light grey with a shghtly brown tint. It splits into small,
thin, conchoidal slabs on the planes of deposition, which are very obscure.
The contact lines above and below are very sharply defined. Sometimes the
bed is divided into two or more layers, and the proportion of clayey matter
is not quite untform. The only fossil observed in the water-lime, or cement
rock was found in the upper layer at the southeast end of the Solvay Process
Co.’s quarry at Split Rock. This was an impression of one of the thoracic
seoments of an Hurypterus measuring two and nine-sixteenths inches im length,
seven-eighths of an inch at the ends and one-half inch in the middle. It
showed the segment to have been slightly pustulose.

The peculiar property of hardening under water possessed by this lime-
stone when calcined and pulverized, was discovered about the year 1818

during the construction of the Rome and Salina section of the Erie canal. A

PLATE VII

SYRA

ILES SOUTH O

M

TWO

ED; BRITTON AND CLARK’S QUARRY

ORA B

TROMATOP¢

3)

HE

DAer)
Pat

ic

Luraer—Economic Gronogy or Ononpaca Counry. 269

quantity of what was supposed to be ordinary quicklime, from the “blue
lime” beds of the Helderberg escarpment persistently refused to slack on
the application of water, as required in the usual process of making mortar.
This cireumstance led Judge Benjamin Wright and Canvass White, civil
engineers employed on the canal, to thoroughly examine the rock strata and
they employed Dr. Barto, of Herkimer county, to assist them in a series of
experiments which resulted in the knowledge of the great value of hydraulic
cement, and of the method of preparation and the character of the strata
from which it is derived. It was first used on the canal in 1819, and sub-
sequent to that year all of the masonry on this construction was laid in
water-lime. It immediately took rank as an important resource of Onondaga
county and maintains that position to the present time.

The quarries from which the cement rock is taken, are usually located
near the top of the Helderberg escarpment, where the superjacent beds of
limestone are comparatively thin. After these have been removed and utilized
as building stones or made into quick-lime, the hydraulic limestone is loosened
by blasting-powder and heavy bars, and broken into pieces of as nearly uni-
form size as possible and convenient for handling, then loaded on cars or carts
and hanled to the kilns. The kilns are egg-shaped wells, ten feet in diameter at
the top, twelve feet in the middle, three and one-half feet at the bottom, and
twenty-eight to forty-two feet deep, with an opening at the bottom, from
which the contents can be taken out at will. There are usually several kilns
built in an embankment of very heavy masonry, so constructed against a
hillside that the raw material can be conveniently conveyed there from the
quarry, and burned lime easily remoyed from the bottom of the kiln.

Great care is used in the selection of the material and the construction of
the kilns, to enable them to withstand the long continued fierce heat. Onon-
daga limestone is most commonly used, Oriskany sandstone occasionally.
Generally, but not always, a lining of fire-brick is put in. When a kiln is
ready to be filled, a cord of dry, hard, four-foot wood is put into the bottom
and covered four inches deep with coarse anthracite coal, then a layer one
foot thick of the limestone, succeeded by another layer of coal, partly coarse
and partly fine. This is repeated till the kiln is filled to the top, which
requires about ten tons of coal and fifteen cords of stone, equal to 1,500
bushels of lime. Then the fire is started at the bottom, and gradually works
its way upward until the whole mass is glowing with heat. After two or
three days the gate or door in the bottom is opened, and through it the lime,
now in ragged clinking masses, is drawn to the amount of 250 to 800 bushels

270 Report oF THE STATE GEOLOGIST.

per day, fresh coal and rock being constantly added to keep the kiln
full to the top. This is continued as long as desired, or until repairs are
needed.

The material is next taken to the mill, where it is reduced by stone
crushers, especially constructed for this purpose, to such a degree of fineness
that it can be fed evenly through a hopper to the millstones where it is pul-
verized to the fineness of flour. It is now hydraulic cement, and ready for
use. It is shipped in buik, or packed in barrels or sacks.

Although the two layers previously described comprise all of the water-
lime rock of commercial value in this county, the quantity of raw material in
sight and convenient of access is practically unlimited. One cord of stone
makes 100 bushels of cement, and the output can easily be increased to meet
all demands.

The following are some of the principal producers :

Thomas W. Sheedy. Mill and three kilns one mile north of Fayette-
ville; quarries on Dry hill, southeast from Fayetteville: also buys raw
material. Output, 15,000 barrels.

Bangs & Gaynor. Mill and four kilns at Fayetteville, quarries on Dry
hill, and buys raw material. Output, 40,000 barrels.

James Beahan estate. Mill and four kilns one mile north of Manlius, by
the side of the Chenango branch of the West Shore railroad; quarry 100 rods
south of mill. Output, 50,000 barrels.

A. E. Alvord, of 223 E. Water street, Syracuse. Nine kilns and large
quarries on the east side of the West Shore railroad, at Manlius village. The
mill is at Syracuse. Output of cement, 45,000 barrels.

Brown’s quarry, operated by Eaton Bros., at Edward’s falls, on West
branch of Limestone creek, one and one-half miles southwest from Manlius.
Mill with water power and one kiln. Output, 7,500 barrels.

Robert Dunlop, one-half mile north of Jamesville, has five kilns, and a
mill run by water power on Butternut creek; quarry on the hill east of the
works. Output, 80,000 bushels.

KE. B. Alvord & Co. have a mill and two kilns in the village of James-
ville; quarry one-half mile south of works on east side of Butternut creek.
Output, 21,000 barrels. This firm has large quarries and four kilns on the
west side of the valley near the reservoir, at which operations are suspended
at present. ‘

Britton & Clark have a mill and seven kilns near the Delaware, Lacka-
wanna and Western railroad, at the north end of the Jamesville rock-cut. The

“AMUVNO SMav1ID GNV NOLLIYG NI YSAV1 SWITYSLWM SHI

IA 31W1a

LutHer—Economic GroLoGy or OnonpaGa County. et

rock is brought down in cars by gravity from the quarry, which is 100 rods
‘south of the works. Output, 100,000 bushels.

L. H. Walker has a cement mill, run by water power, near Marcellus
falls. ‘The kiln is on the east bank of the creek, and the quarry at the top of
the bluff behind the kiln. Output, 3,000 bushels.

P. C. Corrigan has a mill and two kilns at Skaneateles falls, and two
quarries, one on each side of Skaneateles outlet. Output, 12,000 bushels.

In H. E. Alvord’s quarry, at Manlius, the top of the upper layer of
hydraulic limestone is forty-six feet, four inches below the bottom of the
Oriskany sandstone, which appears in the low bluff a short distance east of
the principal excavation. This space is occupied by dark bluish or black

bituminous limestones in “runs”

or layers from one to nine feet thick, of
the same general character as that next below the water-lime courses. The
layers are usually separated by thin seams of carbonaceous matter.

At the foot of the hill west of the cemetery, one mile south of Onondaga
valley, two thin, non-persistent nodular layers of chert occur. No chert was
observed elsewhere in this horizon. Several species of fossils occur in these
beds, though not all that are found in the upper layer appear in the lower.

In Alvord’s quarry, a layer nine feet, eight inches thick at the thickest
place, forms the “cap” of the quarry. It is exceedingly rough and scragey,
and very striking in appearance. It is composed largely of the fossil Stvoma-
topera, and is very pure, making, when burned, a very superior quality of
quicklime. This layer is very persistent, appearing prominently at every
exposure of this horizon, except in the vicinity of Split Rock. The fossil
is very abundant also in many exposures in strata below the water-lime
courses. At Severance’s gypsum quarry, in Dewitt, it may be seen not more
than fifteen feet above the top of the massive bed of gypsum. Leperditia
alta, Spirifer Vanuxemi, and Stropheodonta inequistrialis, also occur above
as well as below the water-lime layers. The upper layers at Manlius con-
tain several species of corals, cyathophylloid and favositoid, and a few
brachiopods.

At Jamesville, in E. B. Alvord’s quarry, on the west side of the valley,
there are thirty-one feet of limestone between the upper water-lime bed and
the Oriskany sandstone. Stromatopora is very abundant through the upper
twenty feet.

At Britton & Clark’s, south of Syracuse, on the east side of Onondaga
valley, the same strata have a thickness of twenty feet. On the opposite side
of the valley, two miles west, they are eleven feet, six inches thick, and at

272 Repor? OF THE STATE GEOLOGIST.

Split Rock, the water-lime layer is separated from the grey Onondaga lime-
stone by only two inches of coarse lumpy shales.

At Walker’s quarry, at Marcellus falls, five miles west from Split Rock,
eleven feet of fine dark limestone intervenes, which at Corrigan’s, at
Skaneateles falls, six miles further west, has increased to twenty-one feet,
nine inches, and the Stromatopora bed, two feet, six inches thick, appears in
characteristic form.

Economically considered, at least, all of the limestones lying between the
gypseous shales and the Oriskany sandstone belong together. A large
majority of all the quarries in the county are located in this horizon. From
the purer layers, especially the Stromatopora beds locally known as the
“diamond rock,” is derived all of the quicklime produced in the county, and
the whole group furnishes an unlimited supply of easily worked, durable
building stone and road metal that is easy of access, and contributes very
largely to the prosperity of the county, and gives employment to a large
number of its citizens. The Lower Helderberg or “blue” limestone is used
principally as cellar or foundation stone, the Onondaga or grey limestone
being generally preferred for cut work and dimension stone. Grace church on
University avenue, Syracuse, and St. Mark’s church, in the western part of
the city, both handsome edifices, are built of this rock in broken ashlar,
trimmed with hammer dressed Onondaga limestone. The large flouring mill
at Manlius, the Onondaga county almshouse at Onondaga Hill, and many
other buildings used for business purposes or as residences were constructed
of stone from these beds. It is much used also for road making, as it breaks
easily into sharp angular fragments, making excellent material for that pur-
pose, and for mixing with cement and sand to make concrete. A. E. Alvord
has a steam crusher at his quarry on the north side of Rock Cut, near the
Delaware, Lackawanna and Western railroad, which gives employment to
seventy-five men. The output from this plant last year was 27,000 cubic
yards. Britton & Clark’s annual output averages 5,000 cubic yards, and it
is produced in smaller quantities at several other quarries where it is broken
with hammers.

The process of manufacturing quicklime from the “blue lime” layers is
the same as that employed in making cement from the water-lime layers,
except that it is not necessary to grind the calcined rock, as it slacks on
the application of a suitable quantity of water, and becomes a fine white
powder, and is then ready for use. Some of the principal producers of

quicklime are:

‘NOLHOING YVSN “WeVID GNV NOLLIYG 40 TIIW LNSW3S0 GNY SNTIM AWD

y O09 GuOIMVYO MOSENATIVH dOOMNAM

XI SLV1d

i

Luraer—Economic GroLoGY oF ONONDAGA County. DAt a

H. E. Alvord of Syracuse, quarry and kilns at Manlius. Annual out-
put, 200,000 bushels.

James Beahan estate, quarry and kilns at Manlius. Output, 75,000 bushels.

FE. B. Alvord & Co., Jamesville, 50,000 bushels.

Britton & Clark, Rock Cut, 50,000 bushels.

All of the limestone used by the Solvay Process Co., of Syracuse, in the
manufacture of soda-ash, amounting to more than 250,000 tons annually, is
taken from “blue lime” beds in the large quarry operated by the company at

Split Rock, about five miles southwest from Syracuse.

Very little blasting powder is required in quarrying these beds for

building stone. In the flexing and tilting to which they have been subjected,
they have been much shattered, owing to their rigid, brittle character, so that
vertical cracks, joints and crevices are very frequent. By the use of heavy
pinch bars large blocks are dislodged. These are roughly reduced with
heavy hammers to such sizes and shapes as may be desired, then hauled to
their destination where the facing stone or ashlars are finished with chisels
and light hammers, the rest being laid into the wall without further dressing.

During the century of occupancy of this region by white men, a very
large number of quarries have been opened along the line of outcrop of these
limestones, at first, to supply local demand in the building of the villages
which sprang into being when the Seneca turnpike was the great east and
west thoroughfare across the county, following very closely the brink of the
great escarpment. Some of them were abandoned, but a large number of
new ones, more conveniently situated in regard to transportation, were opened
when the building of the Erie canal and the railroads and the rapid growth
of the city of Syracuse created a new and immense demand from another
direction.

The following are the names of the owners of quarries who produce

building stone from the “blue lime” beds:

meeesivord,;Manlius .:... . . . io LO0OuCords:
James heahan estate, Manlius ...... 200. &
ieeeiverd & Co. Jamesville... . . . 250°:
Rover Dunlop, Jamesville... . . . . . . . 100. “
imoema Olark,-Syracuse*. . . .. . .-. 2500
Isaac Cole, East Onondaga. . . Bptia) ipaen ry L000 <
enn Connolly, Hast Onondaga... . . . 1500 &
Sere wussell): Rast Onondaga':°. i... 20 .--1000 ¢
George Redhead, Hast Onondaga ... .'. 500 ¢

18

274 Report oF THE Stare GEOLOGIST.

Patrick Knox, East Onondaga, . . . . . . . 50 Cords
L. C. Dorwin, Dorwm Springs, . . . 5 ae s
D. McNeil, Street’s quarry, Onondaga hill, ss 1500 “
John Kearny, North of Onondaga hill, . . . . 200 “%
Solvay Process Co., Split Rock, . ..... ZS

Oriskany Sandstone.

The line of separation between the top of these limestone beds and
the base of the superjacent formations, is very distinctly marked. A
thin seam of arenaceous brownish shale, or sof¢ sandstone, which weathers
out and crumbles away on exposure, separates the fine dark limestones from a
bed of coarse, light grey, sometimes pinkish sandstone, which is nodular in the
lower two or three inches, and usually has flattish pebbles of dark rock
embedded in it, but is compact above. In some localities it is well cemented
and durable, at others it turns dark-colored and crumbles easily. Its position
in the escarpment is well toward the top, and generally only the edge of the
layer is exposed.

At Manlius, the lower fourteen inches of a layer two feet, three inches
thick, 1s characteristic Oriskany, gradually changing to a calcareous sandstone
and then to a pure blue-grey limestone, identical in appearance with the
overlying Onondaga limestone. At Alvord’s quarry southwest from James:
ville, it is a layer of friable sandstone, weathered to dark brown. At Britton
& Clark’s and at Russell’s, it is substantially the same as at Manlius. It is
exposed, and large loose blocks abound, on the side of the hill a short distance
southwest from L. C. Dorwin’s quarry, one mile south of Onondaga valley.

Tlere it is a pure sandstone, very light grey with a pink shade, containing
many impressions of fossils, Spér/fer arenosus largely predominating. The
stratum 1s here four to four and one-half feet thick. In the Street quarry
north of Onondaga hill, it appears at the west end as a coarse conglomerate
about six inches thick. At Split Rock, there is but a trace of it in the seam
of nodular calcareous shale which separates the blue lime from the grey beds.

At Walker’s quarry, Marcellus falls, a layer of granular limestone
five feet, three inches thick, is arenaceous toward the bottom, the lower
four inches being characteristic Oriskany. The whole layer is brownish
grey after exposure. It is very remarkably developed im the northern part
of the town of Skaneateles, on the mdge east from Marysville. It is well

exposed above Corrigan’s quarry as an unusually clean sandstone, very light

"AYYYNO WOOY LIdS SHL NI ANOLSSWIN VOVONONO SHE

X Jivd

Pi a

lé
Ve

Lurner—Economic Grotocy or OnonpaGca County. 275

grey or pink, weathering white and containing, especially toward the bottom
of the beds, impressions of great numbers of Spirifer arenosus and associated
fossils.

The greatest thickness observed in this county was eighteen feet at this
place. Good exposures occur a mile or two northeast, and in the vicinity
of the road leading from Skaneateles to Elbridge. Vanuxem states its
thickness here to be thirty feet. Fragments, large and small, easily recognized
as from this bed, are found scattered over the fields clear to the south line of
the county. Mr. Graham says that in the Tully salt wells the Oriskany sand-
stone is fifteen to eighteen feet thick, light-colored, coarse and gritty, wearing
away the corners of the drills so that they “get out of gage” and make a
smaller hole.

The economic value of the Oriskany sandstone to this county is not great.
It was quarried in the town of Skaneateles and used in the construction of
the lock on the Erie canal at Jordan, also for cellar and foundation stone, and
occasionally for lining in lime kilns, The proximity of the Onondaga hme-
stone which can be worked much more cheaply appears to be the main cause
of its disuse.

Upper Helderberg Group.

The strata of this formation are represented in this county by a bed of
light grey, glistening, semi-crystalline limestone, separated by thin seams of
carbonaceous shales into layers from an inch to two feet, six inches thick,
and which maintain their character and thickness over large areas. Many of
these layers are compact and composed almost entirely of calcic carbonate,
but others, and they are not confined to any particular horizon, are shaly
and contain more or less argillaceous matter. Both the compact and the
shaly layers contain fossils in great abundance, especially corals and crinoids.
Many species of brachiopods and gasteropods are common everywhere in the
beds. Flattened nodules of dark bluish black chert or hornstone, some-
times in continuous layers, also occur throughout the entire mass, though
more common in the upper part.

At Manlius, in Alvord’s and Hinsdell’s quarries, a layer of chert occurs
im the stratum of limestone superjacent to the Oriskany sandstone: also
in the lower layers at the Reservation quarry, and at every exposure of
the Onondaga limestone as the lower part of the formation is frequently
called, as well as in the upper part to which the name Corniferous was given

on account of the presence of the hornstone. The rocks of this epoch have

Report OF THE STATE (GEOLOGIST.

to
“I
or)

a total thickness in Onondaga county of about sixty feet at the eastern
boundary, increasing to seventy feet at the western. At the Tully wells they
are seventy-five feet thick, according to Mr. Graham who superintended the
drilling. The Corniferous limestone is the surface rock over a narrow belt
at the top of the Helderberg escarpment, rarely showing more than a few
feet in the face of the cliffs, though at the west end of the great chasm of
the Green lakes, two miles north of Jamesville, the upper twenty-five feet
of the vertical wall is of Onondaga lmestone. At Dry hill in Manlius,
along both sides of Onondaga valley, at Split Rock, and in fact at almost

every exposure it has been worn away, almost or quite, to a thin edge, evi-

See
—_— ~ —S ———

=== SS ———
Sous Lh —————e ————————

Salina Red Shale —— —————_ — —_ — —— a

East

Figure 8. East and west section across Onondaga county, showing the position of the lime-

stones in the Helderberg escarpment.

dently by glacial action, as glacial polishings and grovings are abundant. By
reason of its elevated position it was subject to the full power of the denud-
ing forces, and huge blocks were torn loose, tossed about and scattered im the
wildest and most fantastic manner. On the hillsides along the north and
south valleys, immense limestone boulders abound for many miles, and some
were carried to the tops of the highest hills. The window and door sills of
the stone store at Pompey hill were cut from a large block of Onondaga
limestone found a short distance away. on the very summit of the hill, six
miles south and at least one hundred feet above the bed from which it was
torn. The line of outcrop extends for the entire width of the county, with

elongations toward the south along the sides of the valleys. East of Manlius,

‘ISAM ONIMOOT 'AYYVNO YOOY Lids SH]

IX 31W1d

ODGH od Myo HOSENS TVA GOOHNAM

Luruer—Economic Grotogy oF Ononpaca Counry. 277

en Dry hill, there is a large area where the rock is bare or but slightly
covered ; also northwest from Jamesville, in the vicinity of the Green lakes,
and about Split Rock.

The Corniferous limestone is of great economic value as a building stone.
It is strong and durable, can be quarried without difficulty and dressed into
any desired shape, as it is soft and tough under the chisel and dressing
hammer, It is capable of receiving a high polish. It is bright looking,
clean and handsome, and does not fade or change color on exposure, and
is abundant without limit. Many large buildings in the county are con-
structed of this stone, and it is used very extensively for trimming and
ornamenting brick buildings. Large slabs of it are used for flagging on the
principal business streets of Syracuse. It is much used in monumental
work in the cemeteries, and for curbings, hitching posts, horse blocks and
the like.

Quarries near Manlius and at Split Rock supplied large quantities of
heavy cut stone for locks and culverts along the Erie canal, as far west as
Rochester, where it was used in the construction of the aqueduct across the
Genesee river, and from these and the numerous other quarries which have
been opened all along the ledge, has been taken the material for the bridge
abutments, culverts and other stone work required in the building of the
several railroads which intersect the county, and also the highways in the
vicinity.

Operations have practically ceased in a large number of the grey lime
quarries, and the business is confined to a few of those most favorably located
in regard to accessibility and cheapness of transportation into Syracuse. The
manner of quarrying the Corniferous limestone differs somewhat from that
employed in the blue limestone quarries, and is substantially as follows:

The soil and shale or undesirable rock is “stripped” or cleared away
over the surface of the layer to be used. Lines are then drawn which
indicate the size and shape of the block or slab required. Along these lines
a row of holes one inch in diameter, and four to six inches deep are drilled,
a foot or less apart, a “wedge and feathers,” two half-round pieces of iron, are
then inserted in each hole, and the wedges carefully driven so that the strain
shall be uniform for the entire length of the line and until it is sufficient to
cause a fracture. The slab is then removed by the use of large derricks, and the
process is repeated. The blocks and slabs are generally, but not always, hauled
from the quarries in the rough state; the smaller ones to stone yards where
they are dressed and the heavier ones to the places where they are to be used.

278 Report OF THE STATE GEOLOGIST.

The largest quarry now in operation in the Corniferous limestone is at
the Indian Reservation in the Onondaga valley, three miles south of Syracuse.
Kelly Bros. operate the principal part of it. They employ thirty-five men,
and their annual output is 12,000 cubic yards. Patrick McElroy works the
south end of the quarry. He employs eight men a part of the year, taking
out 750 cubic yards during the season. The section exposed here embraces
thirty-seven feet, four inches. The bottom is about five feet above the
Oriskany sandstone. The top layer is shaly. Fossils are exceedingly abun-
dant at these quarries, especially in the shaly layers.

In the Solvay quarry at Split Rock, the Corniferous section shows at
the southwest corner, twelve feet, ten inches of compact or shaly layers of
limestone with shaly partings. Dimension stones are quarried from the
compact layers. John Kearney, near Onondaga hill, quarries 1,250 yards
annually, and Job James, in the same locality, 250 yards. A. E. Alvord owns
a large quarry one-half mile east of Manhus, where the section shows seven-
teen feet, six Inches of the lower part of the Corniferous limestone, nearly
all of which is in compact layers of convenient thickness.

There are several other grey lime quarries in the yicinity of
Manlius, but the expense of transportation precludes extensive operations
at present. E. B, Alvord & Co. operate a small quarry at the base of the
Corniferous limestone, one mile south of Jamesville, on the east side of the
Reservoir. William Maylie’s quarry, one-half mile southeast from Marcellus
village on the Cedarville road, is in the upper layers of the Corniferous, as
are also John Clancy’s and Martin Hogan’s in the same vicinity.

The section in Maylie’s quarry shows seventeen feet, two inches. At
the top, four feet, three inches is shaly and very fossiliferous; the other layers
are quite compact. Several thin nodular layers of black chert occur.
Some of the lower layers of limestone are quite bituminous and very dark
colored, but weather to ight grey. The cut stone for the dam at the foot
of Otisco lake was taken from Maylie’s quarry. Mr. Maylie also burns quick-
lime, running one kiln, Nodules of iron pyrites in some localities very
injuriously affect the value of these upper beds for building purposes, but at
these last mentioned quarries the rock is quite free from it. John Keenan’s
quarry a few rods south of Corrigan’s, at Skaneateles, shows about four feet
of hard limestone next to the Oriskany sandstone, and above that five feet
of shaly limestone in which are a few hard layers three to four inches
thick. The material for the Glenside mills was quarried near the mills.
J. H. Ketchum’s quarry one-half mile south of Skaneateles falls near the creek,

LSva

SNIMOOT ‘AYYHVNO WOOY LiIndS SH]

>

WX ALW1d

Luruer—Economic Gronocy oF Ononpaca Counry. 279

in the horizon of the middle of the Corniferous strata, shows a section of
twelve feet in even compact layers one to two feet thick. One layer of black
chert two inches thick is persistent.

Many prominent buildings in the city of Syracuse have been built of
Onondaga limestone. Among them are the Onondaga County Court House,
on West Genesee street, built in 1857; St. Mary’s Cathedral, built in 1874;
Reformed Protestant Dutch Church, on James street, built in 1884; May
Memorial Church, on James street, built in 1884; St. Paul’s Cathedral built in
1884; the Post-Office building, on East Fayette street, built in 1884; the W.
S. Peck block, on West Water street, built in 1887; the City Hall, on East
Washington street, built in 1892; the Onondaga County Savings Bank,
corner of Salina and Genesee streets; the Hall of Languages, Syracuse Uni-
versity ; Senator Horace K. White’s residence on James street, one of the
most elegant in Syracuse, is built of medium-sized blocks of grey limestone,
jaid in broken ashlar style.

Hamilton Group.

Overlying the Corniferous limestone, and constituting the surface rock
over nearly all that part of the county south of the great limestone ledge,
are the soft shales and fine thin sandstones of the Hamilton group, the
lowest division of which is the Marcellus shale, so named because of its
favorable exposure in the town of Marcellus. The transition is abrupt, the
black shale being in immediate contact with the grey limestone below. In
the lower seven feet it is more or less calcareous owing to the presence of
immense numbers of a minute pteropod, Styliolina fissurella, and at one
horizon indurated, forming a thin, non-persistent layer of very dark laminated,
unpure limestone. Except in these calcareous portions, where they are blue-
black, the shales are very bituminous and fetid, black with a brown streak, and
become rusty on exposure by reason of the abundance of iron in their com-
position, and fissile, with very thin laminae. Fossils, especially Lvorhynchus
imitaris, ave quite abundant in some of the calcareous layers. Thirteen feet
above the top of the Corniferous limestone there occurs the layer of hard,
dark impure limestone, about two feet, six inches thick, known as the Gonia-
tite limestone on account of the abundance and great size of this fossil.
The stratum is usually composed of two layers, the lower one the thicker.
Adjacent to the shales the limestone is compact and even, but in the middle
part it has the appearance of being concretionary, and when broken presents

a rough, scragey surface.

280 Report or THE Srare GERoLoGist.

The fossils are most abundant in the lower part of the upper layer.
Specimens of Goniatites Vanuremi, which show the original adult shell to
have been from eight to twelve inches in diameter, are common; also orthoce-
ratites, two inches in diameter and a foot long, and many other interest-
ing fossils.

The limestone is slightly exposed on the hill east of Manlius village,
south of Eagle, but very much better in the southwest corner of the town of
Manlius, along the Jamesville turnpike. In a small ravine near the school-
house in District No. 8, at a fall about fifty rods from the road, the limestone
is well exposed, accessible, and very rich in fossils. It can be traced along
the ridge toward the west for nearly a mile, though this being a region of
fexures, it is easily lost sight of.

It crops out near the highway a mile northwest from Onondaga hill, also
along the road between Loomis hill and Howlett hill. There are several
outcrops between Marcellus and the Onondaga valley near the Cedarvale
road, and also on the road between Marcellus falls and Marysville.

Next above the Gomiatite limestone is a bed of fissile shale or slate,
forty to fifty feet thick, black and ferruginous like that below, but not
calcareous, and very rarely containing a fossil. Inregularly disposed in this
bed, though more abundant at some horizons than others, are many large
concretions, some of them very symmetrical flattened spheres, while others
are elongated, nodular and frequently geodic septaria.

The shale above gradually loses its slaty, bituminous character, becoming
softer and more argillaceous, the color changing to a bluish grey, the concre-
tions smaller and less abundant. The change is so gradual that any line of
separation between the Marcellus shales and the Hamilton shales must be an
arbitrary one. It has been placed at 200 feet above the Corniferous lime-
stone, which is a liberal allowance for the thickness of the Marcellus. Neither
the limestones nor the shales are of appreciable economic value.

All the experience of men who have spent time and money in the
vain search for coal in these beds has not even yet entirely destroyed the
belief that it exists in large quantities, the belief resting on the presence of
occasional thin seams of coaly remains of plant life, and the general carbon-
aceous appearance ot the shales.

The Hamilton shales and sandstones are the surface rocks over an

area equal to about one-third of the county—an area embracing the southern
parts of the towns of Pompey, Lafayette, Onondaga, Marcellus and Skaneateles,

and the northern parts of Fabius, Tully, Otisco and Spafford, and ex-

WDVONONO Lsvg ‘AYYVNO ST1SSSNYy 'SNOLSSWIT SNOYSSINYOD

WX SLW1d

Lutarr—Economic GroLogy or ONONDAGA Counrry. 281

tending into the deep valleys of Skaneateles, Otisco and Tully lakes,
Labrador creek, Keeney’s creek and Limestone creek, quite to the southern
boundary. Throughout this entire region of high hills and deep valleys,
the rock is generally but thinly covered with drift, and the soil is largely
composed of disintegrated shales, especially along the sides of the hills.

At the base of these Hamilton strata is a mass of soft argillaceous shales,
brownish or bluish grey, with layers of olive or light blue color; some thin
layers are bituminous. Calcareous concretions are not uncommon. — Fossils
occur sparingly in the lower part, but more and more abundantly toward
the top.

The thickness of this part of the Hamilton group, which embraces the
Ludlowvyille shales, is between 300 and 400 feet. It is exposed in the Lime-
stone creek valley, north of Delphi; also in the vicinity of Watervale, and in
the Butternut creek valley, m the vicinity of Onativia station, in the Onon-
daga creek valley north of Cardiff, and in many places in the southern parts
of the towns of Marcellus and Skaneateles.

A large portion of the upper Hamilton rocks is composed of soft
shales, similar to those just described, but intercalated with them are beds
of coarser arenaceous shales and schistose sandstones in which fossils are
exceedingly abundant, masses of them supplying calcic carbonate sufficient to
cement the loose and rather friable material into firm hard rock. These hard
layers frequently appear on the sides of the hills, forming terraces and escarp-
ments distinguishable for long distances, and show plainly the southerly dip
of the strata. These terraces are developed to a remarkable degree on the
sides of the valley of Onondaga creek south of Cardiff, where six can be
distinctly seen on the west side. One of them rises as a bold escarpment on
the hill west of the village of Delphi. Several occur also on both sides of
the Otisco valley south of the lake, and in many other places.

The sandy layers are exposed at the top of Pratt’s falls, and between
there and Pompey hill, and at Conklin’s falls and Delphi falls, in Fabius in a
ravine west of the dam at the foot of the DeRuyter reservoir, also in the
valley between Fabius village and Keeney’s settlement. The ravines about
Cardiff and in the vicinity of the Tully salt wells are excellent places in
which to examine them and to collect fossils, and the same is true of the
Otisco valley, particularly at the mouth of the Bucktail ravine. ‘The
Whole series of the upper Hamilton shales and sandstones is well exposed
at the south end of Skaneateles lake in the numerous ravines, and along
the shore.

232 Rerorr or tHe Srare GEoLoaist.

On the east shore, two and one-half miles from the head of the lake, near
Staghorn point, is a very remarkable bed of fossil corals. It is a solid mass of
cyathophylloid or cup corals, together with other genera. It is five feet thick at
the thickest place, and is exposed along the shore, near the level of the water,
for a distance of a quarter of a mile or more. Thousands of specimens, some
of them ten or twelve inches long, and sufficiently suggestive of staghorns to
give the name to the point, are in sight in the layer or loose in the water. This
coral reef, or a similar one at about the same horizon, is exposed at Lord’s hill,
several miles northeast, and along the hillside west of Otisco lake. From
its position it seems probable that this bed is the eastern extension of the
Enerial band of the western counties, which ‘abounds in cyathophylloid
corals of the same species.

At the top of the group there are about fifty feet of soft dark shales,
which contain iron pyrites and become rusty brown on exposure. Calcareous
concretions and thin non-persistent calcareous layers composed entirely of fossils
are common. The color and character is maintained, though the beds become
thinner, as far west as Livingston county, where they form the upper ten feet
of the Moscow shales. A good exposure of this horizon is by the roadside, one-
fourth mile north of Tully centre, on the upper road. Another is at Tinker’s
falls, near Labrador pond ; also on the dugway road, from Spafford village to
Skaneateles lake. The Hamilton shales have had a very important part in
the composition of the fertile soil of Onondaga county, but the direct economic
value of the group is very small, and’ is confined to a few of the sandy layers
that are durable enough to serve as building stone.

Pompey Academy was built in 1834, of stone quarried on M. Beard’s
farm, one and one-half miles north of Pompey hill, and the material for the
two stone buildings used as stores were from the same quarry. Another
quarry on the Dowlett farm, one-quarter mile southwest from the same
village, suppled the stone for the Dowlett residence, and the brown-grey
slabs, covered with impressions of large lamellibranchs and brachiopods, have
been built into all the cellar walls and stone fences in the vicinity. The
material for the dam at the foot of the DeRuyter reservoir was quarried from
a hard layer near the west end.

The Tully limestone, the last division of the rocks of the Hamilton
group, is composed of several thick layers of hard, light blue limestone and
intercalated beds of calcareous shales, which appear in the southern tier of
towns, and separate the brown-grey Hamilton shales from the black Genesee

slates. Some parts of the limestone are quite pure and even grained, but the

. ID
: 5 VIVH AL
ISNOVYAS
NO » LIANG
S3SWNIN YOYVGNON(
AINOLS3Y

tic“.
~

ee le

“

LurHer—Economic GroLOGY OF ONnonpdaéAGA Counry. 283

larger portion, though quite hard, is a lumpy, rubbly mixture of limestone
and a small amount of clayey matter, which breaks easily with a very irregular
vertical fracture, and on exposure is inclined to crumble. At most exposures
the upper and lower layers are shaly. It 1s exposed on the hillside west of
the Tully lakes, where it forms a sharply defined terrace, which gradually

rises toward the north into a bold escarpment nearly 100 feet high. It has

Figurn9 The Tully limestone section at Carr’s quarry, Tully, N. Y.

been quarried for building stone and burned into lime at this place. At
Carr’s quarry, the upper shaly part is covered; the thickness exposed is
twenty-three feet, four inches. Barrett’s quarry near by is not now operated.
The Solvay Process Co. quarried in this ledge for stone used in building the
dam and gateways at the foot of Crooked lake. Ousby’s quarry, one-half
mile east of Tully village, is not operated, and but a part of the limestone is
exposed.

YR a)
284 Report oF THE Strate GEOLOGIST.

There are no other good exposures of the limestone in the eastern part of
the county, but at Tinker’s falls, just over the line in Cortland county, near
Labrador pond, it forms the crest of the fall, which is sixty feet high and
projects over the shales beneath in the shape of a crescent, which is eighteen
feet wide in the middle. The upper part is hard limestone, mostly rubbly ;
the lower ten feet, nearly all shaly. The total thickness exposed is twenty-
nine feet, six inches. There is a small outcrop in the southeast corner of the
town of Fabius.

The terrace reappears, though less distinctly seen, on the north side

of the Vesper ravine, and continues with one interruption—that of the Otisco

creek—to a point about one mile northeast of Otisco centre, where the out-
crop on the Kingsley farm is the most westerly exposure in the county.
According to Mr. E. B. Knapp, the limestone is twenty-two feet thick, and
its altitude 1,500 feet, A. T.

In the Bucktail ravine, near Spafford Hollow, the Tully limestone is the
crest of a high fall, and it is exposed in a small ravine near by. It is also
exposed near the highway one mile southeast of Borodino, where it is unusu-
ally rich in fossils, one horizon being a crumbling mass of sections of crinoid
columns, and orthoceratites a foot long and two inches in diameter occur.
The strata here are in a disturbed condition, as though they had been under-
mined and had fallen with a sliding movement. The Nunnery schoolhouse,
one-quarter of a mile south from this exposure, was built fifty years ago from
Tully limestone quarried near by.

From this point south along the east bank of Skaneateles lake, it appears
in several ravines. Where the highway crosses the ravine, above Colonel
Jeaney’s cottage, there is a fall and a vertical exposure where, including a
few feet above the bridge, the limestones measure thirty-two feet, ten inches.
An excellent exposure for examination is in the dugway road leading up from
Spafford landing. An outlier, which is quite extensive, occurs in the hill
north of the village of Tully. The limestone is exposed near the mill dam in
the bed of the small stream that runs through the village. It would seem
from the elevation and position of Pompey hill, that the Tully limestone

should be found there, but such is not the case.

Chemung Group.

All the rocks of the Genesee epoch and that part of the Portage
epoch which includes the lower Black band and the second Black band,

as those formations appear in Ontario and Livingston counties, are repre-

‘SNOLS3WIT YOYONONO JO LIINg

“ASNSVYAS '1L33YN1S SAWYE 'SLIHAA 3DvH JH 'N

a EE

=. * i

Lurner—Economico GroLtoGy oF ONonDAGA CouUNTY. 285

sented in Onondaga county by a bed of bituminous black shale with slaty
Jaminw, which is exposed to a small extent in the high hills in the south
part of Fabius, Tully and Spafford, with a spur extending into the eastern
part of Otisco, and an outlier in the southern part of LaFayette. Fossils,
except plant remains, are exceedingly rare, and concretions, so abundant at

this horizon further west, are seldom seen in this county. There are few

- good exposures of the entire section. One, however, occurs in the road lead.

ing up from Spafford’s landing on Skaneateles lake. The bed here is
ninety feet thick. It is exposed in the ravine east of Ousby’s quarry, near
Tully village, and the upper part in “ King’s gulf,” one-half mile south of
Ousby’s. The upper part is somewhat less bituminous here than at Spafford.
Outerops of this bed occur at various places on the sides of South mountain

[| Tully Lakes

Skoaneoteles Coke

Ficure 10, The east and west rock section along the southern boundary of Onondaga county.

in Fabius, and considerable time and money has been expended in digging
into it, in the vain belief that, beyond exposure, it would be found to be coal.
Nothing of economic value has yet been discovered in these black slates.

In the absence of any well defined line of separation between the Genesee
slate and the Portage shales in the western counties, this bed of black slate
may be assumed to belong to the Genesee. The light colored Portage shales
with flaggy layers and thin sandstones are the surface rocks over the steep
sides of the highest hills in the extreme southern part of the county, and also
occupy a part of the high plateaus usually found at the summits. About
twenty feet next above the Genesee slates are soft light bluish or olive shales,
some layers fissile, others blocky, non-fossiliferous so far as known. Above
these, eighty-five feet of rather hard blue shales with a few thin sandstones 1
which no fossils were observed, then a bed of sandstones and hard shales.
At “King’s gulf” these sandstones contain Aulopora in large quantities,

286 Report oF THE Strate GEOLOGIST.

besides Spirifer, two species of goniatites, etc. Above this is a succession of
hard, sandy, bluish shales and thin bedded sandstones, aggregating 155 feet in
thickness. The sandstone layers in the upper part of this division have been
quarried for flagstone near the village of Spafford. In some of the layers of
shale which separate these sandstones at the quarry, specimens of Strophomena
mucronata and a small Orthis are quite abundant, and other species occur
sparingly. This quarry is 260 feet above the top of the black shales, and is
in the Ithaca beds of the Portage group. This horizon is not exposed in
King’s gulf, but near the top of the hill directly east, in the highway lead-
ing from Tully to Truxton, a layer of sandstone crops out which contains many
Chemung fossils. This layer is 265 feet above the Awlopora beds and 370
feet above the top of the black slate. Overlying it and outcropping in many
places, are hard shales and sandstones, which cap all the high hills on the
southern boundary line of the county, the greatest thickness being 300 to 350
feet, all belonging to the Chemung group. Although these upper sandstones
are suitable for building stones, and in some places for flagging, they are not
quarried. The loose blocks and slabs scattered about the fields supply the
demand, which is entirely local.

The quarry at Spafford was operated vigorously at one time, and pro-
duced some very fine flagging, which was taken down the hill to Spafford’s
landing, thence to Skaneateles by boat. It is not now operated. A factory
located at Manlius manufactured whetstones from a layer of Portage sand-
stones in Labrador hill, or South mountain. They were called “ Labrador
stones,” and had a large sale, but their manufacture has ceased. Many flags
from the Aulopora beds may be seen in the sidewalks in Tully. They were

quarried a few miles south, at Preble, im Cortland county.

Quaternary Era.

The deposits of the Quaternary era consist of the earlier drift material
brought from the north, with additions from the local limestones and shales
carried by a southward movement and spread over all the south part of the
county, even to the tops of the highest hills, where granite boulders and
blocks of Medina sandstone, together with Lower Helderberg and Onondaga
limestones, are common. This drift is generally coarse and unassorted, and
the few beds of sand or clay found in sheltered positions are small and of
little importance.

The valleys of Limestone and Butternut creeks in the town of Fabius,

and of Onondaga creek in Tully, are choked hy immense deposits of unstrati-

‘SSIVHS NOLIWYH ‘S14 IHd135q

IAX 3LW1d

OS a40aM—o 103ENI71V

HdOONNA

i
‘
&

Lutier

Economic Gronoagy oF OnonpaAGA Counry. 287

fied drift to the height of 1,250 to 1,300 feet, A. T. The Limestone creek
has cut a deep gorge through the mass between the DeRuyter reservoir and
Delphi. A large deposit of this character near Apulia separates the waters
of Butternut creek from those which flow southward to the Tioughnioga
river. The Onondaga valley in the town of Tully is closed by a mass of
drift piled in great disorder to a height of 400 to 450 feet. The surface is
very uneven, especially on the west side, and the Tully lakes lie in the
depressions, some of them draining into Onondaga creek, and others into the
west branch of the Tioughnioga. The mass is unassorted gravel, usually very
coarse, containing a large proportion of limestone pebbles and boulders, with
other material brought from farther north.

Here and in all the higher parts of the county, sand, suitable for build-
ing purposes, is found only in small isolated deposits, which are well distrib-
uted, however, and sufficient for the requirements of the inhabitants. The
most important sand beds are those along the sides of Onondaga valley,
between the Indian Reservation and Syracuse. They are from fifty to one
hundred feet thick, the top of the formation being a little more than 500
feet, A. T.

On the east side, in the vicinity of Brighton, the deposit is very
large, varying in quality from fine sand suitable for stone work to the coarser
erades and fine gravel. At Dorwin’s springs on the west side, there is a large
deposit at the north end of a broad terrace which extends out into the valley,
and there are others farther north. Digging out and hauling the sand into
the city of Syracuse furnishes employment for a considerable number of men.
Some of the principal owners and dealers are :

L. C. Dorwin, who leases his sand pit, from which are taken annually
25,000 cubic yards.

Benjamin Clark, pit near cemetery south of Onondaga valley; output,
1,000 cubic yards.

Frank Patterson, Brighton, 6,000 cubic yards of sand, of which 2,000
cubic yards are shipped out of county ; ‘also sells 2,000 cubic yards of grave)
annually.

George Kleinheinz, Brighton ; 3,000 cubic yards annually.

James McComb, Brighton, 300 cubic yards annually,

Hugh Scott, Brighton, 600 cubic yards annually.

Samuel Irving, Brighton, 200 cubic yards annuaily.

Lucian Cross, Brighton, 400 cubic yards annually.

Richard Crandon, Brighton, 400 cubic yards annually.

288 Reporr oF THE Stare GEOLOGIST.

The principal part of this sand is used in the construction of buildings,
cement sidewalks, and pavements in the city of Syracuse. The Adamant
Plaster Co. uses 4,000 cubic yards; the Eureka Plaster Co. uses 4,500 cubic
yards, with capacity recently increased to 7,000 cubic yards; and the Paragon
Plaster Co. uses 6,000 cubic yards annually in the manufacture of wall plaster
prepared ready for use, which is to a large extent shipped out of the county.
In the northern towns good sand is found abundantly sufficient for local use,
though no large deposits were observed.

Clay beds of the Champlain epoch occur in ail the valleys in the county
south of the Ime of the limestone outcrop. Many of them show by their red
color that they were derived, in part, at least, from the Salina shales. A
large deposit of this stiff red clay occurs at the south end of the Onondaga
valley in the vicinity of the salt wells, at a distance of seventeen miles from
the nearest present exposure of the red shales and 200 feet higher. University
hill in Syracuse, is partly composed of the red clay, generally mixed with
fragments of shale and limestone. In the middle of Onondaga valley, in the
southern part of the city of Syractise near Brighton and Midland avenues,
there is an extensive deposit of clay which is owned by the Syracuse
Pressed Brick Co. It is on the flat in the middle of the valley, at an elevation
of about 450 feet A. T. » When the alluvial soil which is eight to twelve inches
thick is removed, a bed of reddish brown clay two and one half to three feet
thick is found, from which bricks of a rich dark red are made. The next one
and one-half feet below includes the irregular contact line between the upper
bed and the second one, and this material is made into ordinary building
bricks which are of various shades of red or buff, and sometimes mottled. The
second stratum of clay from the top is three feet thick. It contains less iron,
and bricks made from it are light buff. They are burned hard, and like the
dark red ones from the upper layer, are used as facing brick.

The lower bed is dark bluish brown, and is made into ordinary building
brick. The company employs forty men and _ fifteen boys during the season.
The output in 1895 was 4,000,000. This company has recently purchased 113
acres of land east of the city on which are large clay deposits, and expects in
the immediate future to manufacture on a large scale bricks from these beds.

On the north side of the city just beyond the corporation line there are
several brick yards. The owners are:

Preston Bros., 7th and North streets; employ eighteen men. Annual
output, 2,000,000,

G. W. Peck & Son, 7th and North streets; fifteen men. Output, 1,500,000.

‘USAIN VOSNSS AHL NO ‘390INSMAN LY

"ANWdINOD ONIAVG GNY MOING WMYOA MAN AHL 4O $aQ3e AVID

i pas “

ie

WAX 3LW1d

LurHEr—Economic GroLocgy oF OnonpdAGA County. 289

John Brophy, Brewerton Plank Road; fifteen men. Output, 1,560,000.

F. H. Kennedy, 7th and North streets; ten men. Output, 1,000,000.

C. & L. Merrick, Whiskey Island, out E. Court street; thirty men. Out-
put, 3,000,000 and 500,000 ornamental pressed. brick.

The Onondaga Vitrified Brick Co. at Warner’s, manufacture $5,000 worth
of roofing and drain tile from clay beds adjoining the works.

A clay bed about 200 acres in extent lies west of the railroad station ‘at
Jordan. Edward Heighhoe owns eleven acres of it, and manufactures drain
pipe and horseshoe tile to the value of $2,000 annually, and employs three men.

One hundred thousand bricks are made annually from a bed in the vil-
lage of Baldwinsville.

On the east side of the Seneca river, one-half mile north of Newbridge,
is situated the bed of stratified clay several acres in extent and at least twenty-
five feet thick, from which is obtained the material used by the New York
Brick and Paving Co., of Syracuse, in the manufacture of vitrified bricks for
street pavements. The top of the bed is twenty feet above the river, and
has an elevation of, 885 A. T. It is covered by two feet of sandy loam. The
upper part is,composed of nearly level layers of clay four to six inches thick,
brown or pinkish in the middle, becoming lighter colored toward the upper
and lower surfaces, and which are separated by a thin light drab layer one-half
to one inch thick, composed of very fine white sand, generally, but not
always, mixed with a little clay, which produces a characteristic and striking
banded effect. When a mass falls over from the vertical walls of the
excavation the clayey layers separate on the sandy planes and slide on each
other like flagstones. This part of the bed is ten to twelve feet thick. Beneath
it the clay is of a bluish brown. The lines of bedding are less distinct, and
are much flexed and folded. It has been excavated to the depth of twelve
feet without reaching the bottom. Concretions are quite common in some of
the more calcareous layers three to five feet from the top of the bed. The
most common form is that of flattened spheroids, two to four inches in diam-
eter and one-half to one inch thick. Generally faint traces of a slender root
can be seen in the center. In many cases only an outer rim one-half to one
inch wide has become indurated, the interior having been affected only to the
extent of a slight discoloration that appears in the form of narrow brownish
concentric bands. Besides these curious and rare ring concretions, other sym-
metrical forms occur, that are solid and composed of thin concentric layers.
Occasional irregular accretions of calcareous material about some small central

object are to be found throughout the entire bed.
19

9 1
290 Report oF THE SratTeE GEOLOGIST.

A brickyard was started by Ammi Crawford in 1829, at this place, long
known as Brickyard Point. Tile and a small amount of pottery were made
here about 1846. Since the organization of the New York Brick and Paving
Co, the clay has been transported to Syracuse by canal and manufactured
into vitrified or paving brick, without the addition of any new material, by
the ordinary method employed in making bricks for building purposes,
except that the application of a higher degree of heat is required.

The following analysis of this clay was kindly furnished by Mr. J. L.

Breed, general manager of the company :

Silica, sets Mae tee oe Oe ate i ae ree
Alumina, 32-55 2o 4 ee ee
Sesq: ox: Irony: 6c 08 sue OPAC rari eee ae 3.369
Ox. Manganese, Fig TRL y SA a are Foon a 185
Magnesia, PP <(j--3S a Bie See ee 3.468
Time, 2 1 ee ee 9.298
Organic matters =): 202-554. ee TE
Potassa, Sa SSS ee ee 296
Lossy. 22. 2 srs "05, Sa ee O10
100.000

The company employs forty men. The annual output is 10,000,000
bricks, of which 8,000,000 are used in paving streets and 2,000,000 in build-
ings. Five miles of the streets of Syracuse are paved with these brick. The
company also manufactures acid proof brick and tile for the lining of digesters
used in the manufacture of paper.

Deposits of marl and marly clay are found in the towns of Fabius and
Tully in the vicinity of the lakes, ponds and swamps, the calcic carbonate
being derived from the large amount of comminuted or pulverized limestone
in the drift. Marl is found in large quantities in and about all of the small
lakes in the limestone section of Dewitt and Manlius, and in Onondaga and
Cross lakes. Cicero swamp contains a very large bed, and others occur in the
marshy tracts in the towns of Dewitt and Manhus. Other large deposits of
an exceptionally pure quality have been found in Camillus, Elbridge and
the southern part of Van Buren, near the Erie canal. The marl from some
of these beds is very pure calcic carbonate. When made into bricks and
burned it makes exceedingly white, clear lime. It has been utilized for this
purpose to ashght extent, and it has been considered as of some value as a

fertilizer. Its chief economic value at present is due to the fact that it is the ~

“AGISYSAIY Lv SGSE AID

09 dHOAMYYO HOISNATIVH d(OOMNAM

IAX 3LW1d

LurHer—Economic GroLtoGy oF ONnonpAGA Counrvy. 29]

principal ingredient in the composition of “Portland” cement, which is an
artificial water-lime, having the property of hardening or “setting” under
water.

The American Portland Cement Co. has a plant in the town of Elbridge,
two miles east of Jordan, and owns fifty acres of mar] and clay lying on both
sides of the Erie canal, and another bed of marl near Jordan station. The
marl bed at the works is from eight to fifteen feet thick, and has the appear-
ance of a bed of pure white clay. Entire specimens of recent fresh water
shells are very abundant in it, and also in the bed of marly bluish clay beneath
it, which is the other important component in the cement.

The process of manufacture is briefly as follows: After the muck has
been carefully removed, the marl is dug out and conveyed to the works, where
it is thoroughly mixed by machinery with water and a definite proportion of
clay, together with a small amount of other material, and pressed into the
form of long rough bricks. These are placed on small platform cars, in layers
crosswise, with a space between to allow circulation of air; then taken to a
large room through which is driven a strong current of air heated to a tem-
perature of 150°, where they are rapidly dried and become hardened so that
they can be hauled. They are then placed in large circular kilns, with alter-
nate jayers of coal and subjected to a high degree of heat for three days.
When sufficiently cool, stone crushers and mill stones reduce the calcined
mass to the consistency of fine flour. It is then ready for use.

The American Portland Cement Co. at its Jordan works has twelve
kilns and employs seventy-five men. It manufactures 2,500 barrels of
cement per month. In the town of Camillus, one-half mile south of Warners,
the Empire Portland Cement Co. owns extensive marl and clay beds and
manufactures Empire Portland Cement on a large scale. The marl bed one-
half mile west of the works is six to seven feet thick, covered by two to
twelve inches of black muck. Beneath the marl is a bed of bluish marly
clay two and one-half feet thick. Steam is employed in excavating the marl
and clay and hauling the loaded cars to the works. This establishment turns
out 400 barrels of finished cement per day and employs 110 men. The large
plant of the Warner Cement Co., located on marl and clay beds one mile west
of Warner’s, is not in operation at present. Nearly all of the cement produced
in the county is exported. The amount of marl and clay in the county
adapted to the manufacture of artificial cement is practically unlimited.

Deposits of carbonate of lime in the form of travertine, sometimes

called “basswood limestone,” “horse-bone” and “ petrified moss,” derived

292 Report oF THE STATE GEOLOGIST.

from the same sources as the marl, are common throughout the county except
in the northern tier of towns. These deposits are usually found where some
subterranean stream of water surcharged with lime carbonate comes to the
surface, forming a spring around which, as the water is evaporated by exposure
to the sun and atmosphere, the travertine is deposited, sometimes with earthy
and vegetable matter, but frequently free from them. The proximity and
abundance of lime in more convenient forms deprive this material of the
economic value it might otherwise have.

Masses of conglomerate, or “hard pan,” formed by infiltrating calcareous
waters depositing lime carbonate in sufficient quantities in beds of gravel or
coarse sand to produce cementation, are common. A remarkable instance is
exposed in Hopper’s glen, near Onondaga valley, where a small stream has
cut through a bed of very coarse gravel fifty feet thick, which is so firmly
cemented that it does not disintegrate on exposure; but as the softer material
beneath it has been removed by the action of the stream, it has fallen into
the ravine below in enormous masses. Some of the larger are thirty to forty

feet in their longer diameter.

Condition of the Rock Strata.

The general southward dip of the strata, about forty feet per mile, is
apparent without the use of instruments. Except in the vicinity of the
limestone escarpment, the undulations which are of frequent occurrence are
low and long, for that reason easily escaping notice, unless observed along the
shore of a lake where comparison with the level surface of the water brings
them more plainly to view. Approaching the line of the great outcrop of the
limestones from either the north or the south side, it is found that the flexures
are sharper and more numerous, and that along the entire length of the
escarpment in this county, and including a belt three to five miles wide,
evidence of profound moyement and disturbance of the strata appears at
nearly every exposure. Vertical faultings of more than a few inches were
not observed, but overthrusts producing dislocation of the strata to the
amount of several feet, anticlines with extensive longitudinal fissures at the
summit several inches wide, chasms and jointings, are numerous.

In Beahan’s quarry, near Manlius, as shown in the south wall, the strata
dip to the southwest for twenty rods at the rate of three feet per one hundred,
then for two rods the floor is level to the foot of an inclination that rises for
four rods, one foot in ten, and continues at a somewhat lower angle for some
distance further, covered by drift. One hundred rods south of Beahan’s,

‘"NOLHDING YVSN ‘NYE GNVS S,NOSILLYG

XIX 3LW1d

LurHer—Economic GroLogy or OnonpdAGA Counry. 293

in Alvord’s grey lime quarry, a fissure four inches wide has been worn at
one point to a foot im width, by the surface water that poured through
here to unknown depths below; and thirty rods east of the quarry occurs
a chasm three or four feet wide, partially choked by dislodged blocks of
limestone. By the side of the railroad midway between Beahan’s and
Alvord’s lime kilns the summit of an anticlinal fold in the upper part of the
Gypseous shales is exposed; and near Tod’s gypsum quarry the magnesian
limestones of a low ridge have been extensively flexed and fractured. On
the south side of the road leading from Manlius to Jamesville, near its cross-
ing with the town line of Dewitt, the top of the Corniferous limestone is
exposed in the bottom of the ravine near the schoolhouse, and in another
ravine one-half mile to the west. A steep upward inclination toward the
south beginning near the road is continued twenty-five or thirty rods, elevating
the strata at least sixty feet.

In Britton & Clark’s quarry a thirty-foot section of an anticline shows
several vertical fissures, the widest being eight inches, extending below the

mn
Ua,

He
his

vu
MT

HH}
}
Uy
Mf
Yj

FIGURE 11, Overthrust flexure and fault in C. H. Russell’s quarry at East Onondaga,

bottom of the quarry. At C. H. Russell’s quarry near East Onondaga, the
floor at the west end shows a fine syncline, and at the opening in the south
yall near the east end, the fracture plane of an upthrust fault is exposed.
The dip of the fracture plane is twenty degrees toward the south, and the
displacement of the strata is forty-two feet. The floor of the quarry south
of the fault for about one hundred feet is level, then dips to the south again
at an angle of twenty-eight degrees, twelve feet to the end of the excavation.
The wall of House’s quarry south of the old arsenal at East Onondaga, can be
seen from the opposite side of the valley, showing the arched strata of an
anticline. At the Reservation quarries, the limestones show little disturbance
except near the southwest corner. In the vicinity of Bellevue heights, the
magnesian limestones where exposed are folded and broken, and at Decker
street there is a fissure ten inches wide filled with brecciated travertine. At
Split Rock the strata are but slightly folded, though some wide and deep

2994 Report oF THE Strate GEOLOGIST.

fissures occur. A mile southeast from the village of Marcellus, in the deep
valley leading toward Cedarville, the top of the Corniferous limestone is
exposed over a large area, and the undulations are very apparent.

In Wm. Maylie’s quarry at this locality, an overthrust fault displaces the
strata two feet, two inches. The dip of the fracture plane is eighteen and
one-half degrees. This quarry is three miles from the north edge of the
Helderberg escarpment.

Walker's quarry near Marcellus falls exposes a north and south section
200 feet long, in which the limestones dip toward the south, thirty-six feet.
At the north end of the quarry, which is near the summit of the anticline,
there is a fissure two feet wide, and six rods north another, now partially filled
with large blocks of. limestone, that is four feet wide.

All of the quarries above mentioned are in the Corniferous and Lower
Helderberg limestones, and the flexures and fractures described are in the
upper part of a bed of hard rocks 250 to 400 feet thick.

On the north side of the escarpment, the rocks of the Gypseous shales
and the horizon of the salt beds, wherever exposed, are in the same disturbed
condition, but the most apparent effect of the flexing is the reduction of the
thin bedded or shaly limestones of that horizon toa loose mass of uncemented
breccia. In grading a street in the western part of the city of Syracuse a bed
of limestone was found to be so finely broken to the depth of five feet that
it was plowed without difficulty.

The well known exposure on Green street, in Syracuse, in which appear
the eruptive dikes of peridotite is the most interesting one in this connection,
and perhaps in the whole county.

The high ridge that separates the Onondaga and Butternut creek valleys
extends from Tully to the southeastern part of the city of Syracuse, ending
one-half mile north of the University of Syracuse, which is situated on the
terminating slope of the ridge, at an elevation of about 600 feet A. T. At
the foot of the slope is an alluvial plain three-fourths of a mile wide, having
an elevation of 402 feet A. T. On the north side of this plain there rises to
the height of 150 feet an elevated, uneven tract bounded on the west by the
Onondaga lake basin, and extending two or three miles toward the north and
east. On the south side the slopes are generally quite steep, but more gentle
on the west and north sides. This elevated tract has the appearance of being,
and doubtless is, composed largely of drift material, but in the southwest
part of it, at least, the bed rock lies near the surface, though there are no_

natural outerops. In an effort to modify the grade of Green street north of

'SSNOVYAS ‘IIH 13SYNLS N33YD NO ayia (ALMNeaaWIy) SLiLoai¥ag SHY

>

Luruer

Economic Gronoay or OnonpaAGA County. 295

Lodi street a few years ago, a cut was made exposing a section of the m cks,

200 feet long and 12 feet high at the highest point.

velow the
street grade, enlarging for a few days the exposed section to that extent. The
rocks uncovered are the thin bedded and shaly magnesian limestones that
oceur immediately above the horizon of the rock salt beds, and lie on the
southwestern slope of an anticline, the outlines of which are obseured by the

drift. They are much flexed and broken by the eruption of the materi

In the fall of 1895, a ditch for water mains was dug seven feet |

al com-

HIGHLAND ST,

N .SALINA ST

BURNET AVE

CANAL ST.

Figure 12. The location of the peridotite dike in the city of Syracuse.
a A )

posing the dikes. The principal dike is twelve feet, four inches wide at the
surface of the road bed, and approximately the same to the bottom of the
dike. Above the sidewalk the width increases to the top of the bank, where
it is twenty-five feet, and a layer eight to ten inches thick is spread over the
surface of the rocks for several rods toward the east, thinly covered by the soil.
Another and much thinner dike occurs about one hundred feet west of the
main one, and there are evidences of two others, also small. The middle por-

tion of the main dike is composed of quite firm and hard, dark green peridotite,

296 REPORT OF THE STATE GEOLOGIST.

but adjacent to the walls and in the smaller dikes and the overflow layer
it has decomposed and is now very soft and friable and greenish yellow in
color. The main dike is exposed also on the south side of Green street, but
for only a few rods south of that point. It extends in a northerly direction
across James street, and has been traced by Mr. P. F. Schneider as far as High-
land street, a distance of a little more than a quarter of a mile.

A water pipe ditch dug near the west line of lot No. 805 James street,
and another on the premises of Mr. Hiscock on the opposite side of the street
exposed, and was excavated through, the decomposed overflow layer of this
eruptive to drab limestone beneath. The excavation for the foundations of a
barn on Green street, six rods east of the main dike, exposed a layer of the
same character, ten inches thick, spread over the shaly limestones. Grading
Elm street, which runs parallel with the dike nearly one-half mile to the east,
has exposed the rocks, and shows that the inclination of the strata corresponds
to the general slope of the hill.

The position of the dikes as exposed at Green street is on the southwest
slope of the hill, and sixty feet higher than the low land at the south. The
elevation increases somewhat toward the north. Evidences of the eruption
have been found in this place, over a section one hundred rods in length
and twenty to twenty-five rods in width,

The occurrence of the eruptive rocks in this region was first recorded by
Vanuxem (Annual Report, 1839; Final Report, 1842) and Beck (1842). The
original locality “on the Foot-street road to the east of Syracuse,” was lost
sight of, and the rock was afterward known only from the few specimens
which had passed into the collections of some of the older educational insti-
tutions. From such material its nature was studied and its eruptive character
demonstrated by the late George H. Williams (American Journal of Science,
1887, and Bull. Geolog. Society of America, Vol. 1). A new exposure of this
rock was brought to notice by Mr. Schneider, in 1895, at DeSono station on
the West Shore railroad, about one-half mile south of Dewitt Center, and
an account of its occurrence and nature published by Messrs. Darton and
Kemp (“A Newly Discovered Dike at Dewitt, near Syracuse, New York.
Geologic Notes by N. H. Darton. Petrographic Description by J. F. Kemp”:
American Journal of Science, vol, 49, pp. 456-462, 1895).

On account of the disturbed condition of the strata, any figures given in
regard to the dip can be only approximately correct. From data gathered
from the records of the Solvay Process Co.’s wells at Tully it was found that

the upper surface of the Corniferous limestone has a southward dip of forty

‘ASNOVYAS ‘WH 133yuLS NBS NO 3yiG (ALNeaSWIy) SLiLodidag SH}

69 d8oIMvs THISSNS AV SOONNAM

Pe a o

IXX SLWe

Lurner—Economic GroLtoagy oF Ononpaca County. 997

feet, seven inches per mile. In Dr. Englehardt’s record of the state well drilled
in 1884 at the south end of Onondaga lake, it appears that the Niagara lime-
stone was reached at 208 feet below sea level. As it appears at the surface
nine and one-half miles north of the well at an elevation of 875 feet A. T.,
there is apparently a dip of 61 + feet per mile. Using the record of the
Gale well on the north shore of the lake in like manner, the result 1s 54 + feet
for the dip of the limestone. This increase of dip is explained partly, at
least, by the fact that the thickness of the red shales and the rocks of the
salt horizon increases rapidly toward the south as shown by the well records.
On an east and west line the dip of the top of the Corniferous limestone is hardly
measurable. By comparison with known exposures in Genesee county it is
found to average ten inches to the mile toward the west for the whole
distance. ‘The average westerly dip of the Tully limestone to Ontario county
is 7 + feet per mile.

So far as can be determined by the data at hand, the rock salt beds have
no dip, but are practically level on an east and west line. Some small gas
springs occur in the vicinity of Skaneateles lake and Otisco lake, and at other
localities in the Hamilton shales, but the quantity of gas is not large enough
to be of commercial value. The amount found in the Tully salt wells was
also slight. Large leases of land in the towns of Lysander and Clay have
recently been made by a company intending to sink wells to the Trenton lime-
stone for gas, but as yet no drilling has been done.

298

Report OF THE STatreE GEOLOGIST.

Table showing the Economic Products of the Rocks, and of the Sand, Clay
and Marl Beds of Onondaga County.

NAME OF PRODUCER.

7, Sheedy

7. Sheedy

T. W. Sheedy

Bangs & Gaynor

Bangs & Gaynor

Lansing & Son

F, M. Severance & Co

James Beahan estate ......-.---

James Beahan estate

A. E. Alvord

A. E. Alvord

‘Alvord: jss2ceese ac) ote

AYE.

A. E. Alvord

A. EK. Alvord

Eaton Bros

Robt. Dunlop

Robt. Dunlop

Robt. Dunlop

E. B. Alvord & Co....
E. B. Alvord & Co

E. B. Alvord & Co

E. B. Alvord & Co

Britton & Clark

Britton & Clark

Britton & Clark

Britton & Clark
Kelly Brosin--aa sees ce eee

P. McElroy

Thos. Coughlin

C, H. Russell

Cash Worden

John Connolly

D. & G. Story

| |

|
| No. |

LOCALITY. PRopucT. | AMOUNT. OF | VALUR.
MEN.|
Fayetteville -........| Building stone. 50 cords | 12) $200
| Fayetteville .......-.| Cement.-..--..- 15,000 bbls. se | 6,000
Fayetteville .......-. Plaster ..--.--- 2,000 tons | 5,500
| Fayetteville --..---..|'Cement.-.----- 40,000 bbls. 25 16,000
| Fayetteville ........- Plaster ......-- 5,000 tons | Bre SEN
| Fayetteville. ........ Plaster -......- 2,000 tons| 5| 5,500
| Fayetteville -...-...- Blasters: so- 4,000 tons | 10 11,000
| Mamnis) ers eee er Cements ae 50,000 bbls. 25 | 20,000
Manlius <j.2-cesmen- Quicklime ....- 25,000 bbls. | --.- 10,000
| Manlius and Syracuse} Quicklime. .--. 200,000 bu. 100 20,000
| Manlius and Syracuse| Cement.....--- 125,000 bu. | ...- 12,500
Manlius and Syracuse Crushed stone -| 27,000 cu. yds. Sete, 31,000
Manlius and Syracuse| Building stone. 200 cu. yds. | ---- 800
Manlius and Syracuse} (alcined gypsum... --- | 3,500 tons | .-.-- 6,625
Mamiliusyeemace eee Cement......-- 7,500 bbis. | | 3,000
Jamesville .......-.. | Cement.....-.. 80,000 bu. 20 | 8,000
Jamesville. ......---- Plaster ...- 2,000 tons ....) 4,000
Jamesville. .......-.- Building stone. 100 cords | ..-. | 300
Jamesvalleneacssoeee Cement... ----.. 20,000 bu. 20 2,000
Jamesvillese =e se-eee= Quicklime. ---. 50,000 bu. -.-- | 5,000
Jamesville. .....---.- Plaster ss seaee 2,000 tons. ..-. | 4,000
Jamesville. ....-----. | Building stone. 250 cords | =| 1,000
| Syracuse ..-...-.---- Cement.-..-----| 100,000 bu. 30 10,000
SyMACUSONecleeietesceisiels Quicklime. ---., 50,000 bu. ---- | 5,000
Syracuse e222. 22... Building stone, 2,500 cords | .... 10,000
| Syracuse .-.-..------ Crushed stone .| 5,000 cu. yds. -.-- | 5,750
| Indian Reservation .-| Building stone.) 12,000 cu. yds. | 35\ | 60,000
| Indian Reservation .. Building stone.|- 700 cu. yds, | 5 3,500
| Indian Reservation - | Building stone.| 400 cu. yds. | 3 1,800
| East Onondaga..---- | Building stone.| 1,000 eu. yds. 8 | 4,500
| East Onondaga .-.--.-- Building stone. 200 cu. yds. 2 900
East Onondaga ...-..- | Buildiug stone. 500 cu. yds. 4 2,250
Onondaga Castle ---. | Building stone. 800 cu. yds. 5 3,500

Luruer—Economic GroLoGy oF ONnonDAGA Counrry.

299

Table showing the Economic Products of the Rocks, and of the Sand, Clay

and Marl Beds of Onondaga County.—Continued.

Sandand gravel

NAME OF PRODUCER. Loca.iry. | PRODUCT. Amount. | oe | VALUE.
| | | MEN. |
John Kearmey -- 22 s0-c aSeeiebioase | Onondaga hill. ...-.. Building stone.; 1,450 cu. yds. 8 | $5,800
Sam/lStreet-.2 co e8as-o2 sees Onondaga hill. .----. Building stone.| 1,500 eu. yds. 10 | 6,000
iy CeDonwin == soecise = secon ee Dorwin springs.-.--. Building stone. 800 cu. yds. 5 3,500
WSaaGrCOlGH oats s<12ces = assess Bellevue avenue .....| Building stone.| 1,000 cu. yds. 6 | 4,500
Geowhedlicad= scm ---- ene -- East Onondaga .----- Building stone- 500 cu. yds. 4 | 2,250
RatnickskKnox: --.stes- = ecoe.s East Onondaga ...--- Building stone. 50 eu. yds. 1 | 225
Solvay Process Co..-........--- OVA yee eer eeeroe || QULCkKIIMel = <1 9,000,000 bu. | 3,000 | 900,000
Solvay Process Co.....-.......- Solvay: .-2hie--5-.--<- Salts at sahp oss. 14,000,000 bu. | ---- | 1,120,000
Solvay Process Co.-...-........ Solway eicecees <ccte Building stone.| 5,000 cu. yds. | ---- 20,000
Winase Maier ---5-)--saa-— 55-5 Marcellus) =. 5 -=- Building stone. 200 cords 2 | 800
COnnEC Lan Cymer camera ese Marcellus. ........-.. Building stone. 50 cords 1 | 200
Man tim= Hogan ence stec. smells Marcellus .......-..-- Building stone. 50 cords 1| 200
Tis EUS WiaIKC ON) aicie cic cia vialreseneinse Marcellus Falls. .....| Cement.....---. 4,000 bu. 3 | 400
Pipi Com COLMO ANG oectcreista weenie = c= Skaneateles Falls..-..| Cement......-. 20,000 bu. 5 | 2,000
To Vly USCti WSS 245 saceao cack Skaneateles Falls, ...| Building stone. 100 cu. yds. 1 500
Oy AAMT NE a cecotenetudeendaoce (HORNE Fone Boo cone Building stone. 50 cu. yds. 1) 200
(Qe IONE Ghsten San a sabecemesae spas Way Said Oreja <retarm oler~ 2 Building stone. 50 eu, yds. 1 200
| de Obi oo S504 cscee oSeasa6usskaoe LOU bye cosneonces SBes Building stone. 50 cu. yds. wT) 200
Nip MG SANE ScABE paeocoebecaade Salt Spr. reservation .| Salt, 1894...--. 3,227, 25432 bu. 258,180.37
Onondaga Brick Co. -=--..-.---- Syracuse & Van Buren| Bricks-..--.-.--- 10,000,000 40 60,000
Onondaga Brick Co...-.....---. Syracuse& Van Buren| Drain tile, ete..}| ....-...---.- 5,000
Central City Brick Co........-.- Syracuse & Kirkville| Pressed brick... 1,500,000 25, 15,000
WahieBrooh ys sek eee aes. Solinahee eos sca Bricks. ..-..--- 1,500,000/ 18 8,250
PSE INCINOWY.of aalo fe awe sioiw's1 Seiare alin geese sees a BLICKS. cas sees 1,000,000 | 10 5,500
N. Y. Brick & Paving Co....... Syracuse& Newbridge} Paving bricks. . 8,000,000 | 40 90,000
N. Y. Brick & Paving Co....--. Syracuse&Newbridge| Building bricks 2,000,000 | ..-- 10,500
GanWiew aC ke ey SOMve ne cee ee nia'-)-te Salamayee ase seca =< Building bricks 1,500,000 | 15 9,000
Preston, BlOSeen= > cies ame ciec aor Selina eeeecine so iccee Building bricks 2,000.000 18 11,000
Syracuse Pressed Brick Co.. --.- SYVTACUSCyn cee cess cues Building bricks 4,000,000 50 30,000
Cadeyey MOLEC. somes saa sees Salimayeeea- cease Building Berges! 3,000,000, 25 18,000
Cures le Merrick: . 22am a- nme =me Salinas seer oes Pressed bricks.. 500,000 | Aged | 6,000
Edward Heignhoe...........-.. Ford ames. Gee fone cee: Wraincghileycs: [eee cel ce ew | 3 | 2,000
Frank Patterson .....-.. See ono IBripabomesse = s--a= = 8,000 cu. yds. | ..-- 7,200

300 Report oF THE STATE GEOLOGIST.

Table showing the Economic Products of the Rocks, and of the Sand, Clay
and Marl Beds of Onondaga County.—Concluded.

ey
NAME OF PRODUCER. LOCALITY. PRODUCT. AMOUNT. | ae | VALUE.
| sa
s . ic oe alle ae
|
Geow Kleinheimnze-2425 see ena Brightonitotete sees. | Sands eee 3,000 cu. yds. | ..-- $2,500
Bu Clarkit ist ose acen tees cet Onondaga valley. .--. Sands se teen | 2,000 cu. yds.) 2222 800
LaCo Dorwits:22s-s. sees. eee _ Dorwin’s springs. --.- TSP haved soe 25,000 cu. yds. |) <= 3: 20,000
Re Crandon ser soe | Brightonmi-too=.----- 5 psandeeeeeeee 400 cu. yds. | ---- 320
Tucan) Cross. 2: yee ee eee | Brightonyes222- -2ee-= Sands em. sa eee 400 cu. yds. | .--. 320
NamuUel Irvine = sacs == ce Seer | Brighton =-22--.----e- Sandss2)2- 22. 200 cu. yds:,} ---- 160
Geon Moores. ss. ce eee eee | Brightonsss-2e- s=-ee6 San diseases 800 cu. yds. } —--- 640
Hu ghiScotteat=-o see eee | Brichtoni-.sses--esee Sand soe. es 600 cu. yds. | -.-- 480
American Portland Cement Co..| Jordan ...-.-- are Port?nd cement, — 30,000 bbls. 75 75,000
Empire Portland Cement Co....7 Warner’s ...-..--.--. Portl’nd sent 117,000 bbls. | 110 300,000

: peers
Lururr—Economic Grotoagy or Ononpaca Counry. 301

Summary Statement of the Economic Products of the Geologic Formations
in Onondaga County.

| PRODUCT. VALI.
( Marl beds. | Portland cement. $375,000
Champlain: Periods... 2. =-5+2- Clay beds. Brick and tile. 206,000
| Sand beds. Sand. 33,745
(
| Portage Group.

Chemunp Period: = 225 5-- =: “ Building stone and flagging.
| Genesee Shale.

Tully Limestone. Building stone.
Mamiitons Pernod: ss 7420.2... } Hamilton Sandstones. Building stone.

Marcellus Shale.

Upper Helderberg Period. ..-. Corniferous Limestone. | Building stone. 90,000
Oriskany Beriodia 322. = Steer Oriskany Sandstone. | Building stone.
|
| | Quicklime. 936,000
; Cement. 77,900
Lower Helderberg Period. -_-. Water-lime Group. ¢
Building stone. 42,400
Crushed stone. 36,750
eee beds. Gypsum. 50,000
Onondaga Period-.-.-./--.-.. { Salt beds. | Salt. 1,378,180
|
|
| Salina Red Shales. Brick and tile. 87,000
|
Niagara, Limestone. Building stone. 400
Niagara Periode 222... .--22.5- |

\
| Clinton Shales. | 2
( $3,353, 950

302

Table of Elevations.

Report or THE SvarE GEOLOGIST.

| Lor |
Locairy. | Town. | ANS Abe
| No. |
South bill.sco-Uo. ecg ee pitabiuss 22st eee | 34 | 2,020 |
Apulia sR. Statlonic.-----= eee sere Wabiusy- == eee 21 1,227
Well.45 (Group diy. 2s. 25 settesse oaeeeeeee Mullly e223 18 721 |
Well 1, :GroupiA’ ose Sees eee Pullly shoo see 28 901
Ripley hilly Ass 0 sees e tee oo eee Spattondsesseees ase 32 1,968
Ihimestoneé ledges. s--oe eee ee eee eens Spattordas-- essere 12 1,365
Kingsley ’s.2:3- se. satis eee eee eae eee Obiscor hrc esas | 95 1,500 |
Pompey hills sssect ese eee pote eee Pompey. =asen- ce eee | 65 1,742 |
E. (O3'Clapp's farm. 22 Ne aeeeree aera ere POMPCOY (o-oo ese eee 5 123 |
Cardiffisaltswell.225222)-- eee eee ee eee eee | La Fayette ...-...--- 57 GO1 |
Chas. ‘Carpenters farmis=- soe sane se eee | Onondaga ...--.--... 96 1,105
D. Cossittts fanmi-c- aceon oeeee eee eee | Onondaga. ..---.+--=- 118 1,020 ‘|
Split rock. 23.2052 haces sesaeee eee ewe oe: | Onondaga ....- Se onOA fees 849
Howlettdill:: 6¢ ee eee ee Marcellus...-..------ [Sire ettse
M.Séeley’sifarmic-. 3. -eee saeecee soe er | Skaneateles. .-..-.-.- 22 1,109
WP Giiles}smtanm 23) 5 = see eee | Skaneateles. ......--- 66 1,265 |
Rien Homie setanm asses eeeereae eee nee Skaneateles. .....-.-- | 45 | ~ 1,198
Jordan canal Se so ee eee eee eres ee | Elibridgeseeses--eseee | meee | 409
Jordan, West Shorevhehee as-is ae es = Hibridse.Saeeasee- = Sone | 396
Jordan, NOYoCoRIR eee: [elpeidieg: seer eee ae 401 |
Painmount see ees eee eerie tee Bere aeons | Camilts' === --asce = 36 | 736
M.\Sherwood(stfarm>— seers seseine see ae | Camillus: he sees eee 48 | 799
Dr:-Drapersuarnm .-ceee eee eee eee eee || Geddes =e eee eer=ao=is 150 | 653
N.Y. Cu RR statlonyssseeceecssee ener Syracuse cssseeeee sees acer 403
West shore RoR. Stationetse- sensors eee | Syracsers.ue-2 oes | Eee 400 |
Div Ti. & IWR. Stables eee see cee iS yMACUSC eee eae eee a == 399 |
Brie canal 23.2 S336 ag-eee eee eee Synacuseseee s-.=seen ie 401 |
Mt. Olympus =). =2-)o se eeeSeeee cee Syracuse nese ae senor 187 | 681 |
Chestnmtinidvecs a. .cc-2 -cee oe eae eee | SaLunA fee Stes a= 110 498 |
Collamenr® cc. .tic 0252s seen Soca enero OD Gwe bhtacm caters seteeiore | 12% |) 485 |
[raiGreen’s farm. ..202. :caee ee eee ( MD Stwilb biecteeestee mine 95 | 974
Jamesville Rak station... ee. coe aece eee Dewiltiic.. ot ese stared | 591
Dewitt: contorm.¢- -Samocsecinoseeasenee | TD OWALUD ye ots areyal bei camel Sen gt 410
Bagle shila. 22. tote c cast see eee Man ling 2e eeu ee 79m) 258

AUTHORITY. —

Gardiner’s survey.
Gannett.
Trump.
Trump.
Gardiner,

E. B. Knapp.
iE. B. Knapp.
Geddes.
Gardiner.
Trump.
Gardiner.
Gardiner,
Geddes,

Gardiner.

Gardiner.

Gardiner,

| Gardiner.

Gannett.

Gannett.

| Gannett.

Gardiner,
Gardiner.
Gardiner.
Gannett.
Gannett.
Gannett.
Gannett.
Gardiner.
Gardiner,

Gardiner,

Gardiner.
Gannett.

| Gannett.

Gardiner.

Cro

Seal

ss Lake

=

; "Beaver
We ) Lake

! eye AS tel =

|Newbridge

; — \
Zee 5 :

Aa SS 535
y ¢ e a ZN ~ Baldwinsville
{ f : EXQ@91
NR } =
\

\ \ VAN BUREN

\ ey 641 537

eS AL

Gal

cul |

oo
653

GEDDES)

‘o)
xy
A”

A ake Sodom
ius

me il :
\

PA i || FSS Ss =
f. a, | ee re
| = >
= { bay etlevitle
Bite ' Hoes bette = a :
Falls | 136! AT ; &
; Nos unite! ake

Manlius j
5

Ind An
RésZorvation

Sele)

ne af
Pera alls

2{ my

Ve store

ee i J Bo cae ‘ ne Fall

fee >! ‘) a
Pempey </ ( \
uit Hill Sh me
1265 { 43, AE

va ecoarees.- Via,

eof Miles

cna HALLENBECK,.CRAWFORDCO. NEW YORK & ALBANY.

GEOLOGICAL MAP 2 ONON DAGA COUNTY
By D.D.LUTHER,

feioi>:

LEGEND
| CLINTON SHALES

() Niacara Limestone
RED SALINA SHALES

= [| Grpseous SALINA SHALES
] LOWER HELDERBERG

2 ‘| ORISKANY SANDSTONE

(paz CORN IFEROUS LIMESTONF

: MARCELLUS SHALE

—

HAMILTON SHALE

ce Tu LLy LIMESTONE
() cevesee Suave

ez PORTAGE FORMATION

LuruEer—Economic GEOLOGY oF ONoNDAGA County. 303

Table of Elevations.—Continued.

Loca iry. Town. ae [PAD AUTHORITY,
No.

Kamkewill 6aneetee eens cccce elec ea sece yes MIianilitte ye creciacere ens | 38 507 Gardiner.
Kirkville, N. ¥. C. R.R. station... ------ Miamiliis® see cai) <) eane 423 Gannett.
Kirkville, West Shore R.R. station....--. Manlins \o-ceresc =e hokactins | 422 | Gannett.
Fayetteville R.R. station -...--....-.---- | Manlins....-. BSE OBE ssa | 538 Gannett.
Eye Dawisonisrarms == specie este we tioS -=-2 | Vian ‘Buren's----..---- 42 631 | Gannett.
Chee Ranepley/sitarmt cts. Fe mic a oes | Weamuirenssmicmgno.- 22 | 537 | Gannett.
Mom\phisiea seer eee slo sttaciiee co 5.scb marhas. | Van Buren..--...-... ee 410 Gannett.
Sorrel Eni ete a as ae Oe pees, Bree Van Buren---=-------| 20 | 641 Gannett.
WWATREr sesso a Sys caties cee tinetsc22 | Van Boren ..-....... Was sper | 427 | Gannett.
Me Daviswtanriniass=—- jt ea a ee Diysander..s- -- = | 81 | 5385 | Gannett.
Baldwinsville R.R. station.......---.---- | Deny Samd ere <ces2 = oa | Soe 391 | Gannett.
Es Tih et oo een oe os fps 2s SGN ee) base tes 2M
Skaneatelesilake recon see caencnceten once | acs a ec hee | 8603 ae et Re. ca ae ta
OTISCOMBAKORE NS Aah aacae mer eee eee ose [foe aoe oN ke PF eae | U0Rs Worcedaudiveqseaoncece
Onoudaramakers ceo ersstes Sassen. caee Reet eo on au | ceas) | 361.4 | o.---- ----- 2 no-- =e.
omy WEN). o3scce0 454 2s sbecnadassa5 sane Wee ta ee see | Solan 1190 Trump.
Crookedslakenms2 ees. 35.022 52 Bao Sas ae eet Soe er ata 1,193 Trump.
smlliyaGreenmalkOmacse sects sae ase ee saul wes oce tees eh sco aes [Pog errs 1,191.5 | Trump.
HMakeisodompersetee tee sie c es cctee ee oeeh -ee ce seas aiieete dole Taye AQGUS | eenusctene Soot ae kc

GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

THE STRUCTURAL AND ECONOMIC GEOLOGY OF ERIE
COUNTY.

JAMES HALL, PLR NVUNG SE. BISHOP,

State Geologist. Assistant.

1895.

305

~ ve

ee ae

James Harr, State Geologist,

Sir:—In this report are included the results of geologic studies in Erie
county, N. Y., begun during the summer of 1895 and continued to the close
of that year. The purpose of the investigation was to ascertain the bound-
aries of the formations for the geologic map of the state, and to collect data

regarding economic products derived from rocks found within the county.
Respectfully yours,
IRVING P. BISHOP.
Burrato, N. Y., January 1, 1896.

303

‘SAIVHS YNOVHSYD 4O dOL SHL NO S1S3Y¥ 14357 SHL OL YAld LXSN SHL +: 33SSSN3S5D SHL 4O
dOL SHL NOdN SLS3Y GNNOYSSYOS SIGGIW SHL NI YSld SH{ “SNVAQZ HLYON LY ‘WSSYHO STIN-NSSLHDIZ NI SHOOY SOVLYOd GNV BS3SSSN35

09 dYOIMVYS OSE NET E SOONNAM

| 4LV1d

The Structural and Economic Geology of Erie County.

By Irvine P. Brsuop.

PHystoGRAPHy.

Erie county, in central-western New York, is bounded on the north by
Niagara county, on the east by Genesee and Wyoming counties, and on the
south by Cattaraugus and Chautauqua counties. The western limit is the
international boundary from the lower end of Grand Island, to a point where
the boundary line makes a right angle with a line drawn to the mouth of
Cattaraugus creek. It is separated from Niagara county by Tonawanda
creek and the west branch of Niagara river; and from Cattaraugus and
Chautauqua counties by Cattaraugus creek.

The extreme length of the county, north and south, is forty-three and
one-half miles, and its greatest width is about thirty-nine miles, The land
surface contains 1,071, and the lake portion about 160 square miles, giving
it a total area of about 1,230 square miles.

. Topographically, the county comprises three provinces. They are—first,
a low and nearly level plain on the north, extending from the Niagara river
and ‘Tonawanda creek to the limestone terrace; second, a slightly higher plain
having the limestone escarpment for its northern boundary and extending
southward to a line drawn through Bay View, Spring Brook and Marilla; and
third, a region of rolling hills rising gradually to the height of 1,500 feet or
more above tide, and occupying almost all of the southern half of the county.

The Northern Plain. This plain includes nearly the whole of the town.
ships of Grand Island, Tonawanda, Amherst and Clarence and the northern
half of Newstead. Along the Niagara river the banks form clay escarpments
averaging about twenty feet in height and droppmg abruptly to the edge of
the water. From the top of the bank the county extends southward in an
almost level plam, unbroken by hills or ridges, to the foot of the limestone
escarpment, .

The Middle Plain. The middle plain rises abruptly from the northern
plain, presenting throughout the greater part of the northern boundary an
escarpment of limestone varying from twenty to one hundred feet in height.
South of this, the surface is gently undulating with a few lower hills, gener-

ally presenting smooth surfaces. On this plain, Murder creek, Ransom creek
309

310 Report oF THE State GEOLOGIST.

and Ellicott creek take their rise and flow northward across the lower plain to
Tonawanda creek. The other streams which traverse the middle plain are
Cayuga creek and its branches, Buffalo creek, Cazenovia creek and Smoke
creek, the last three of which have their sources in the hill region to the south.

The Hill Region. The elevated region comprising the remainder of the
county consists essentially of a high plateau gashed by streams which have
eroded much of the original surface and left it a succession of valleys and
ridges.

In the vicinity of Chaffee, East Concord and westward, this tableland has
attained the height of nearly 1,500 feet A. T. From this there is an abrupt
slope into the valley of the Cattaraugus creek, with a more gradual descent
toward the north and west. From the Buffalo and Southwestern railway
toward the lake, the descent 1s very gradual and the surface smooth or gently
undulating, terminating at the lake shore in abrupt bluffs. Along the southern
crest of the plateau and extending into the Cattaraugus valley are immense
piles of glacial debris, giving rise to a peculiarly knolly topography. The
principal streams flowing westward from this region are the Big Sisters creek
and the two branches of Eighteen-Mile creek. In their upper courses these
have steep-sided valleys, and in the lower courses deep gorges with precipitous
walls of rock. The ridges between the streams have smooth tops on approxi-

mately the same level.

STRATIGRAPHY,

The rocks exposed in Erie county range from near the bottom of the
Salina shales to near the top of the Portage group. The members in their

order are shown in the following tz ble:

Portage/eroupiin-\1. ae se = i Upper
SP CNS Lower.
( Genesee slates.
Hamiltonoroupas. seen ~ Hamilton shales.
~ Marcellus shales.
. ( Corniferous limestone.
Upper Helderberg group. . . i non iasadimevisnes
Water-lime group.
Salina group.
The thickness of the above rocks as ascertained by deep borings and

measurements will be given at the close of the chapter on natural gas.

Bishop—GroLtocy or Erte County. 31]

The Salina Group.

The rocks of this group are not well exposed in Erie county, the best
section being found in Genesee county, east of Erie county, where the
Tonawanda creek crosses the outcrop of Corniferous and upper Salina beds.
The creek here breaks over the edge of the Corniferous limestone and
hydraulic limestone, forming the Indian falls. Just below the fall, the rock is
a thick-bedded limestone contaimmg nodules of gypsum and weathering with
a cavernous, irregular surface. Below that, the rock is shale, mostly gypseous
in character, sometimes reddish, but more often grey or bluish. On the
Indian reservation, near the mouth of the ravine, a limited amount of gypsum
is quarried, blue-grey or mottled in color and of fair quality. About half a
mile above the West Shore railroad bridge is an outcrop of red and grey
gypseous shales which continue through the reservation to the iron bridge
near the Indian church. Below this is a stratum composed of hard, thin-

bedded calcareous rock, containing minute lenticular cavities and casts of

“
co)
crystals. The rock exposure extends about 200 yards below the bridge.

Within the limits of Erie, county, the Salina rocks are mostly covered
with drift. The most complete section is found in the bed of Murder creek
at Akron. From Falkirk down to Main street are the water-lime rocks.
Below the railroad bridge, shales crop out in the bed of the creek for two
miles or more. The thickest exposure of these showed three feet of light-
colored calcareous shale, weathering to light pink, beneath which were four to
six feet of harder, greenish shale. A small exposure of shale is reported in
-the same creek opposite the end of the road leading east to the Indian reser-
vation, but I was unable to visit it.

An outcrop of thin-bedded hydraulic limestone occurs on the farm of
Martin Racquet, about one-half mile south of East Amherst near the Transit
road, where it is used for macadam.

On Grand Island there are two outcrops. The more northerly is at
Edgewater, about 200 yards below the boat-landing. The rock here is:

(1) Black shale in the river-bed.

(2) Greenish shales contaiming nodules of gypsum, one and one-half feet.

(3) Light-colored, soft, friable gypseous shales, five feet.

The exposure extends 300 yards down the river-bank.

The other outcrop is at the extreme southern end of the island, where
the river separates into two channels, The rock is a thin-bedded, impure
limestone, weathering like the water-lime, and containing minute lenticular

cavities, Fragments of such rock are plentiful in the drift about Buffalo,

ole Report or tHE Srate GEoLoaist,

and it is probable that this stratum is the source from which these fragments
were derived.

On the Canadian side of the Niagara river, from a point about opposite
Strawberry island to the International bridge, there is an almost continuous
exposure of shales, nearly all of which are more or less gypseous and often
spongy, as if mineral matter had been removed by solution. A short distance
above the bridge, water-lime appears in the river-bed and can be traced to a
pot opposite to, or a little above, the stone church.

The Hydraulic Limestones.

The northern edge of the Corniferous limestone, together with the Onon-
daga limestone and the upper part of the hydraulic limestones, form a ywell-
defined escarpment running in a general southwesterly direction from the
Genesee county line to the city of Buffalo. For the greater part of that dis-
tance this escarpment is approximately parallel to the Bloomingdale and
Williamsville roads, as is seen by the accompanying map. Within the
city it follows the general direction of Main street from the almshouse to near
the New York Central railroad belt line at Rodney and Fillmore avenues.
After crossing Main street, it passes near the corner of Oakwood and Wood
ward to Oakwood and Parkside and enters the park at the stone quarry,
crossing from there into the cemetery at the corner of the iron fence near
Agassiz place. From here it sweeps around in a curve to Scajaquada creek
at Main street bridge, and passes out of sight beneath the drift on the left
bank, about 300 feet below the bridge. By examining sewer cuttings, holes
for telegraph poles and other excavattons, the edge of the Corniferous lime-
stone is found to le between Potomac and Bird avenues on Norwood avenue,

fan)

and appears near the Niagara river at the corner of Auburn and Niagara
streets, where there is a good outcrop. On the Canadian side of the river, the
edge of this limestone should be near the ferry landing. The rock is well
exposed a short distance above.

The hydraulic limestone is usually visible at the base, or north side, of
this escarpment as a stratum of variable thickness in the face of the cliff, but
occasionally forms a terrace ranging from a few feet to 200 yards in width,
and approximately parallel to the escarpment. ‘This terrace is most conspic-
uous between Williamsville and the Buffalo city line. in the Bennett-Pierce
tract the hydraulic limestone is found near the surface as far north as the
swamp, and I am informed by Mr. David F. Day, that it occurs near the sur-

face at the deer paddock in the park. Sewer and other excavations have

Bisnorp—Groiogy or Erin Counry. 313

thrown up this rock along Bird avenue, near Elmwood, and in several places
near the Niagara river in the vicinity of Auburn and Bouck avenues. The
rock is not eroded to its base so that a complete section is nowhere visible.
The thickness has been ascertained from well sections given elsewhere in

this report.

UPPER HELDERBERG GROUP.
Onondaga Limestone.

’ In Erie county, this formation appears as a thin band lying between the
hydraulic limestones and the overlying Corniferous limestone. In color it
‘anges from blue-grey to a very light grey. It varies greatly in thickness,
being from three to five inches at the Main street bridge over Scajaquada
creek, Buffalo; seven feet in Forest lawn cemetery; five and one-half feet in
the park quarry, and thirty-five feet in Fogelsonger’s quarry at Wilhamsville.
At Young’s quarry, two miles further east, it is thirty to thirty-five feet
thick, but thins out rapidly beyond to a thickness of three to five feet.
Speaking broadly, we may say that the formation is concretionary in character,
the deposits at Fogelsonger’s and Young’s being merely lenticular masses of
unusual size. Small lenses a few feet in diameter are frequent and usually
extend downward into the hydraulic limestone without any corresponding
depression above, showing that they had their origin while the latter was
yet im process of deposition. The larger nodules are remarkably rich in
organic remains. At Fogelsonger’s quarry the rock in many places is a solid
mass of cyathophylloid and favositie corals, the latter frequently having their
cavities filled with petroleum and bitumen. Single specimens were noticed
four feet in diameter, and large areas of the quarry bottom showed little else

than these fossils.
The Corniferous Limestone.

The northern edge of the outcrop of this formation is marked by the
escarpment already described. A deposit of drift from ten to fifty feet thick
covers the southern edge, so that actual contact with the Marcellus shales
above is not found within the county. At Corfu, three miles east of the
county line, the borings for gas passed through thirty feet of Marcellus shales.
According to this, the Corniferous limestone should be found about a mile
north of that village. The most southerly outcrop of this Imestone near the
county line is near an abandoned railroad track two miles northeast of

Crittenden. A small exposure occurs on the edge of a marsh just northwest

31 Report or THE Stare GEOLOGIS‘.

of South Newstead. Half a mile below Mill Grove, near a dam across Ellicott
creek, is a good exposure of the same rock, and other outcrops occur in the
bed of the same stream for three miles below and, again, near Wilhelm. The
limestone is found in Cayuga creek at Kieffer’s quarry near the Transit road,
about a mile west of Lancaster, and in numerous places below, the last
exposure being at the end of Clinton street, where the creek unites with
Buffalo creek. The deep wells at the Snow Steam Pump Works near Bailey
avenue and Seneca street, at the Atlas Oil Refinery, and at the Buffalo Chemical
Works on Buffalo creek and Abbott road, all started on the Corniferous
limestone as bed-rock. It is found in the Ohio basin, near the lake, and was
found by the engineers when sinking piles for the Lehigh docks and trestles
near Lake Erie.

The Stagford limestone of the Marcellus formation, is exposed at Wende
station on the Lehigh railroad, one and one-half miles south of Mill Grove.
As this stratum les about twenty feet above the top of the Corniferous
limestone, the boundary between the latter and the Marcellus shales must be
at about half-way between Mill Grove and Wende. An outcrop supposed to
be of this Stafford limestone occurs on the farm of Martin Martin, one-half
mile east of Alden Center, and the drift in the bed of the most northerly
branch of Ellicott creek, near Alden, contains abundant fragments of black
shale as far east as the county line.

At Lancaster, the contact les between the lower bridge and Kieffer’s
quarry. The Stafford limestone crops out in the bed of Buffalo creek,
opposite the end of the Winchester road, and the Corniferous appears at the
junction of the same stream with Cayuga creek, less than two miles away.
Dr. H. U. Williams informs me that a limestone scored with glacial scratches
was uncovered while grading the road-bed for the Buffalo, Rochester and
Pittsburg railroad, some years ago, at the point where it diverges from the
Western New York and Pennsylvania, and the Lake Shore railroads.
Although I did not find the exposure during either of two visits made for
the purpose, the excavations being filled with water, I have no doubt that the
rock in question was the Stafford limestone. When the gas-well was sunk in
South park, less than a mile and one-half southeast, the drill passed through
“about thirty feet of shale below the drift, and then several feet of limestone
and shale mixed ;” conditions which confirm the view expressed.

At Stony point, on Lake Erie, fragments of the jet black shale of the
lower beds of the Marcellus are numerous among the boulders which cover

the beach, showing that they were derived from rocks farther north. The

Brsuop—Grotoay or Erie Counry. 31

boundary between the two formations must therefore lie between here and the
Lehigh docks, and it is very probable that Stony Point itself marks the
extension of the Stafford limestone into the lake. It may be assumed,
therefore, that the boundary between the Corniferous limestone and
Marcellus shales, as laid down on the accompanying map, is a very close

approximation to the actual one.

HAMILTON GROUP.

Marcellus Shales and Limestone.

The best section within the county of the lower Marcellus beds occurs
in the vicinity of Lancaster. In Cayuga creek, just above the lower bridge,
is a layer about two feet thick, of a firm, jet black shale containing some iron
pyrites in crystals and concretions. This is overlaid by a foot or more of
grey limestone which had been mostly quarried out and could not be
accurately measured, From the bridge up to near the Lake Como dam, the
rock does not show. Just below the dam, the black shale crops out,
capped by the Stafford limestone, which was at one time quarried here. A
careful estimate, based upon the thickness of the rock in sight, the fall of the
stream, and the measured height of a dam in the village, shows that the rock
from the lowest visible stratum is from fifteen to twenty feet below the
Stafford limestone. On a little brook running through the centre of the
village, there is a fine exposure of the Stafford limestone. In sight, at the
base of this, is a two-foot layer of jet black bituminous shale, smelling
strongly of petroleum and containing pyritous concretions. Above this are

the limestones in layers of the following thickness :

Lowxrst— 12 inches, containing Orthoceras.
8 « & «
14
10 a
18 a
14 « with a little flint at the top.
14 a
12 He

Total, 9 ft. 4 in.

Above Lancaster, the shales are black, thin-bedded, friable and show

very regular jointing. Farther up, the layers become more calcareous,

316 Report oF THE STATE GEOLOGIST.

forming, at the mouth of Little Buffalo creek, a stratum of impure limestone.
Shales of blue-grey color occupy the bed of the creek at intervals for three
or four miles to the eastward.

Besides the outcrops of Stafford limestone already mentioned, there is a
disused quarry of that stone in the field northeast of South Buffalo station on
the Western New York and Pennsylvania railroad, and fragments of it were
thrown up in digging the sewer and water trenches on the Indian church
road, near Seneca street. The only places where the orthoceratite layers were
noticed are at Lancaster and Wende. Other exposures of Marcellus rocks in
the county are in the bed of Ellicott creek between Wende and Alden Center
and above Alden Center near the Erie gravel pit; also in the southern branch
of the same creek north of Alden village. In Buffalo creek it is in sight at
intervals from the end of the Winchester road to within a mile of Blossom.
It occurs on Cazenovia creek, at the Park just above the Cazenovia street
bridge, and for some distance above the covered bridge two miles farther up
the creek. It was also found in laying the water pipes for South Park, 700
feet east of South Park avenue, at the city line, within two feet of the surface,
and in the bed of a small brook near by. At West Seneca, outcrops occur in
the bed of Smoke creek, between the White’s Corners road and the Western
New York and Pennsylvania railroad, and again on the lake shore at Bay
View. From here it forms the lake bottom near the shore for several miles
up the lake.

Hamilton and Genesee Shales.

The transition from the Marcellus to the Hamilton shales is very
gradual, the shale changing from black to blue-grey through almost imper-
ceptible gradations. There is, however, in several places within the county, a
stratum always calcareous and usually much harder than the rocks below,
which seems to furnish a boundary between the formations.

A inile east of Alden, in the bed of the creek above the culvert is a layer
of impure limestone three and one-half inches thick. Below this, the rack is
asoft shale, having Sty/iola fissurella as its most conspicuous fossil, with an
occasional cephalopod. The layer of limestone is not very fossiliferous, and
has the appearance of some of the Marcellus rock. Less than six feet above
is a shale containing excellent specimens of Spirifer mucronatus and Athyris
spiriferoides. Just above this is a concretionary layer, less than a foot thick,
containing characteristic Hamilton fossils, and immediately over the last a third
calcareous layer, containing the usual Hamilton trilobites, orthoceratites and _

brachioy ods.

‘HONY AHL HONOYHL N3SS SI ‘| 3lV1d NI NMOHS ‘390148 SHL SO Y3ld SNOT SH[ ‘14337 SHL NO WaauO SHL 4O G38 SHL
NI SYVAdd¥V YSAVT VIOIMALS SHL ‘SDG!IYs GVONTIVY YAMOT SHL MOISE SGYVA GSYGNNAH JNO 'SNVAQW HLYON LY M3SYxO STIW-NASLHOIQ NI MAA

OTAHOIMVES HOSENSTIVAOOMN AM

4 4 Py
e s
Lice, Pr

i] 3LW1d

Bisuop—GroLtoagy or Erte Counry. 317

A large fragment of limestone of several tons weight and containing
numerous Hamilton fossils was noticed in Cayuga creek near Town Line. It
evidently had its origin in that vicinity, although the parent rock was not
found.

At Blossom is a four-foot layer of a limestone sufficiently durable for
bridge work. It contains the fossils common to the horizon of the Encrinal
limestone and Moscow shales, including an abundance of cyathophylloid corals.
Examination proved that it lies just above a well-marked Marcellus outcrop.
On.the west branch of Smoke creek, a mile below Windom, a hard calea-
reous shale, eighteen inches thick, occurs in the same relative position as the
preceding limestone. Another outcrop is seen where a little brook crosses the
Mile Strip road about 200 yards east of the Hamburg turnpike. The rock
here is a fairly good limestone. At Bay View the corresponding horizon is
represented by a soft calcareous shale about two feet thick, capping the cliff
a short distance south of the hotel.

While by no means certain of the continuity of this calcareous stratum
throughout the county, in the absence of evidence to the contrary I have
provisionally assigned it to the horizon of the beds termed the “ Basal lime-
stones” by Professor J. M. Clarke, and have used it as a basis of measurement
in determining the thickness of the Hamilton and Marcellus rocks.

At EHighteen Mile creek, near Lake Erie, the Moscow and Genesee shales
have thinned out, leaving the Encrinal limestone near the top of the series,

The rocks here above the Encrinal limestone are:

Blue Moscow shale, resting on the Encrinal, . . 15ft.4in. | =
A layer of iron pyrites + to 4 inch thick | =
< 4 8 ) {eS
sometimes merely a stain of rust, believed to ( 8
. =
represent the Tully limestone. m
L2lin@ Sues. gel sy Oy He ie 2 Ee rr aa
The “Styliola band,” consisting here of
(@) Hard" @aleareousishale) >: . . 13. in,
Wi) ISOS LE pe ee os a 8 ¥
: as ‘ t
(c). Iron grey limestone, containing fish- v
° e . D
plates and crmoid stems, . . . . 4 in. cs

(d). Firm iron grey limestone, composed
largely of Styliola fissurella, . 8 to12in. © 1 ft. 9 in.
iterate eaveiute nih. i. Se LE Et. O In.
Then follow twenty feet or more of olive-green shales with numerous

concretions, capped by black shale extending to the top of the gorge.

318 Report oF THE SrareE GEOLOGIST.

The thin layer beneath the “Styliola band” is blue and contains Hamil-
ton fossils, but is more fissile than the shale below, which contain trilobites.
Mr, A. W. Grabau, who has made a very careful study of this layer, says, it
appears to have the fauna of both the Moscow and Genesee beds, and may be
regarded as a passage formation from one to the other.

The relation of the Encrinal limestone to the Styliola band and
associated rocks at Highteen Mile creek is well shown in accompanying
photograph.

Owing to its position near the upper part of the group and the ease with
which it can be traced, I have selected the Encrinal limestone as the horizon
of reference from which the top of the Hamilton and Genesee may readily be
found. It is easily recognized as a hard limestone, two feet or more thick,
usually stained on the under surface with iron rust from the decomposition of
pyrites, and containing large crinoid stems, some of which are nearly an inch
in diameter. Excepting a few outcrops of the “ Basal limestone,” there is no
other rock in Erie cotinty from the Stafford limestone up to the Portage sand-
stones sufficiently durable for bridge or building purposes. The shales
immediately above and for several feet below are always rich in fossils, among
which cyathophylloid corals and brachiopods, Atrypa reticularis, A. aspera,
Athyris spiriferoides, Spirifer medialis and S. mucronatus, are particularly
abundant. Since it resists the action of water and other erosive influences
better than shales, it is found in almost every gully and ravine which cross
the outcrop. Along the lake shore westward from Eighteen Mile creek, it
forms a conspicuous band in the face of the cliff, dipping beneath the surface
of the water near Pike creek. The Styliola band may be seen above it, the
two limestones approaching each other slightly near the western limit. ast
of Eighteen Mile creek, the Encrinal limestone caps the bluff for a short dis-
tance, and is next seen by the road near the house of Mr. Crocker, about two
miles further on, reappearing again in the face of the bluff beyond. From
here it can be easily traced to Wanakah, crossing the creek near the station
just below the railroad bridge. At Hamburg-on-the-lake it is a half-mile, and
at Athol springs about 200 yards east of the railroad. At Big Tree, it is
exposed in the railroad cutting near Rush creek, and on the banks of the
stream by the farmhouse above. At Windom, it is found for some distance
along the sides of the ravine, being well exposed just above the bridge near
the station and crossing the bed of the brook a quarter of a mile further up.
It is here about thirty inches thick, in two layers, the lower of which is the
thicker, and has three or four inches of pyrites at the bottom, The Styliola

“SYNLOld SHL SO 14457 SHL
NO 3A08Y¥ Naas SI YSAV1 VIOMALS AH] “WaSY¥D SHL NMOG YAHLYVS NAWVL Ma3IA ‘W33NO SJIW-N3SSLHDIZ NI ANOLSSWIT INISONG SHL

“ “O09. 0404MVYI YO3ENITIVH JOOMNAM

Wt 31014

- : = BAS >, oy a ier
res ee ss ee

en

Bisnop—Gronocy or Erie Counrry. 319

band crops out near the road to Duel’s Corners, crossing the bed of a brook
200 yards above the bridge, about half a mile east of Hamburg station. It is
here twelve to eighteen inches thick and lies six feet above the layer of
pyrites representing the top of the Hamilton shales. The pyrites at this
point and at other places eastward, is from two to four inches thick. I was
unable to estimate the thickness of the Genesee, as it was partly hidden by
drift.

The Encrinal limestone crops out in Smoke creek near the plank road, a
mile north of Webster’s Corners, at the top of a fall some thirty feet high.
At Spring Brook it crosses Cazenovia creek just below the dam, appearing on
both sides of the gorge for a mile below. The thickest portion measured
was four feet from top to bottom, with one layer of eighteen to twenty
inches.

The favosite corals here had their cells filled with crude petroleum and
other bitumens so that a tablespoonful could be scraped with a knife from the
surface of a single specimen.

The Styliola band is well shown for a mile above the dam, having about
the same thickness as at Windom. It is here from four to six feet higher
than the top of the Hamilton.

A small exposure of the Encrinal limestone is seen three-fourths of a
mile east of Spring Brook station, where a small brook flows under the track
of the Western New York and Pennsylvania railroad. It is next found
where the covered bridge crosses Buffalo creek, two miles east of Elma.

The limestone crosses the creek just below the bridge, and is quarried
along the bank and on top of the bluff farther down the creek.

The top of the Hamilton shales dips to the level of the creek, one-third
of a mile above the bridge. , The pyrites layer varies from one to four inches
thick, and lies five feet below the Styliola band. The latter is six inches
thick, representing only the upper part. When the concretionary lower layer
appears, as it occasionally does, along the bank, the whole thickness is
increased to a foot and the upper part also becomes concretionary.

The bed of Little Buffalo creek, below Marilla, is filled with drift so that
no bed-rock appears. The Encrinal limestone crops out in the bed of a small
brook emptying into Cayuga creek on the north side near the town line
between Alden and Marilla. It again appears about a mile from Alden
village, south from the station, where the road passes a wood-lot. The rock
has been quarried in a small way near the top of the hill, and an excellent

spring issues from beneath an outcrop in the woods on the other side, a few

320 Report or THE State GEOLOGIST.

rods from the road. Between here and the county line, I was unable to
find any further exposure of this limestone.

Just south of the Erie railroad tracks, a mile east of Alden, is a good
exposure of the Moscow shale with a fauna like that found near the Encrinal
limestone at all points west; and in the absence of evidence to the contrary it
is assumed that this limestone crosses the county line near the New York,
Lake Ene and Western railroad. If so, the Hamilton must be thinner here
than it is east or west of Alden. The Genesee slates in Erie county belong

mainly to the part lymg above the Styliola band, as already shown.

The Portage Group.

The Portage rocks crop out south of the foregoing, to the county line, no
area of distinctly characterized Chemung strata having been observed by me
within the county. The lower part consists of alternations of olive-green
with bituminous black shales, including, rarely, a thin layer of argillaceous
sandstone. Above these, the rocks become more arenaceous, passing somewhat
abruptly into a series of shales alternating with argillaceous sandstones of
varying thickness which furnish stone of considerable economic importance.
The boundary between the upper and lower beds is therefore indistinct. North
of a line connecting Wales Centre, East Aurora, North Boston and North
Collins, no sandstone of consequence has been noticed, and none has been
seen west of the Buffalo and Southwestern railroad, between the latter place
and Gowanda. The streams flowing across the lower Portage outcrop have
cut deep gorges with precipitous sides, but are almost destitute of waterfalls.
The black shales contain many calcareous septaria, usually lenticular and of
enormous size. Specimens six feet in diameter are comparatively common,
and one measured nine feet in diameter by five feet in thickness.

The gorge of Eighteen Mile creek above North Evans, and of Cazenovia
creek below East Aurora, show good lower Portage sections and furnish
excellent specimens of septaria. The southern part of the county is covered
with drift, which in some places is 500 feet or more in thickness. This has
hidden the rock and broken the continuity of observations, so that complete
sections of the Portage rocks like those made in Livingston and Wyoming
counties have not been achieved. The valley of Buffalo creek, above Wales
Centre, shows heavy sandstones and flags as far south as the town line between
Wales and Holland.

Stone is quarried on the Joseph Myers farm, two miles east of Wales

Centre, and also on the Ulrich farm on the Centre Line road, about one and

‘SWV1 SHL WOYS JTIW HLYNOS-SNO 1NOSV NAWVL M3IA “W3S3YS STIW-NS3SLHDIF NO YSAVI1 VIOIALS GNV SNOLS3SWIN IWNIYONG SHL SO SNO/LV1ISY

(O00 GHOIMVYS HOSEN3ATIVH dOOXNAM

; Al 3LW4d

Bisnorp—Gronocy or Erte County. 321

one-half miles southwest of Wales. The two branches of Cazenovia creek
afford the best sections of the upper part of the Portage.

The argillaceous sandstone crops out along the road from Wales Centre
to East Aurora, being quarried a mile east of the latter place on the farm of
W. C. Cook. The layers are from eight to twelve inches thick with the
characteristic surface markings. From East Aurora south, the heavy
sandstones are found at intervals all the way to within a short distance of
Holland. Two and one-half miles southeast of East Aurora, on the farm of
Delavan Caulkins, a quarry is worked by Mr. Henry Strong. The rock here
resembles the Warsaw bluestone and contains the vertical fucoids which are
common in Portage strata. The principal layer is three feet, six inches thick.
Mr. Strong also works another quarry on the north side of the valley, the
stratum apparently corresponding to that in the Caulkins quarry. At South
Wales is the best exposure of sandstone seen. It is located on the farm of
Charles M. Brayton, about twenty rods east of the railroad water tank.
The section here is:

Fiardepine sanastone “=. -. . 3 a Sf Oo feet,
Shale and thin sandstone mixed, about . . ... 20 “
Hard blue sandstone with vertical fucoids . . . Gan act

With thin sandstones and shales above.

Following the railroad south, these sandstones dip below the track at
intervals, the last disappearing at the twenty-fourth mile post from Buffalo,
two miles north of Holland. From here to Protection, the rock observed
is a black fissile shale stained with iron. East of Protection, there is
an outcrop of sandstone with layers a foot thick. Between Chaffee and the
county line, the rock is blue shale with thin sandstones, none of which were
thick enough for flags. This rock has the appearance of Portage. I could
not hear of any stone quarries in this vicinity, although one or two were
reported near Arcade, in Wyoming county.

On the west branch of Cazenovia creek, sandstones occur in several
places, but are generally thinner than those seen on the east branch. ‘They
occur on the higher ground near Jewettville, on both sides of the creek. On
the Phelps farm, two miles southwest of East Aurora, there is also a quarry
of flagstone eight inches thick, from which blocks ten feet square have been
taken. The stratum is comparatively thin, but is near the surface and easy
to work. Below Griffins Mills are several layers from six to eight inches,
with one at least twelve inches thick. A quarry of this stone is worked on

21

322 Report OF THE STATE (GEOLOGIST.

the hillside, about half a mile farther east. Between here and West Falls
there are no sandstones except a few thin flags among the shales. At the
latter place there is a stratum about six feet thick, containing layers like
those at Griffins Mills. From here to East Concord, all the rock in sight
consists of shales and thin argillaceous flags.

A mile northwest of Springville, on the farm of Mr. F. A. Clark, is a
quarry containing a six-foot layer of a grey siliceous sandstone, unlike any
seen elsewhere in the county. In this stone I found several fossils, among
which Professor J. M. Clarke recognized Chonetes scitula, Productella speciosa,
Orthothetes Chemungensis (small variety), and a small Spirifer of the type of
S. mucronatus. These, he says, are representatives of the Ithaca fauna, and
not members of the normal Portage fauna. In the drift near by were
fragments of a small branching coral which may have had its origin in
this vicinity.

On the opposite side of the road, the same stratum of stone is worked in
a quarry owned by Mrs. B. Wheeler. At Pike hill and Townsend hill, three
miles southwest of Boston Corners, are quarries of heavy sandstone, which are
deseribed by Mr. Albert Pike, a former owner, as “ grey sandstone,” and may
belong to the same horizon. Owing to the approach of winter I was not able
to visit these quarries. In the vicinity of Boston and Boston Centre, the
rock is mostly shale with no thick sandstones; but there is a quarry on the
Zeller farm, four miles south of Boston Centre. At the viaduct over Catta-
raugus creek, near Springville, the deep gorge of the river is cut through
olive shales containing very little arenaceous matter.

From Shirley, near North Collins, to Collins, the argillaceous sandstones
occur, being quarried on the farm of Daniel Sherman, two miles north-east of
Collins. They appear to belong to the lower sandstones of the group. At
Zoar, the Cattaraugus creek has cut a gorge through the Portage, exposing
two strata of sandstone. The upper, near the top of the bank, is twenty to
thirty feet thick and separated from a lower fifteen-foot stratum by about
thirty feet of shale. Above Zoar, for five or six miles, the rock along the
river is an olive shale with thin arenaceous layers, but no heavy sandstone.
In the southern part of the county, a fucoid resembling the Spirophyton caudi-

gorge at Zoar.

Cc

galli is very abundant, fine specimens occurring in the

A few poorly preserved brachiopods were noticed in loose micaceous
rock in the bed of a stream near Lawton’s. From the appearance of the frag-
ment the stone had been washed down from the eastward and possibly may

have been derived from adjacent Portage rocks.

‘Siiv4 1SS/\ LY SSNOLSGNVYS 3DvLYOd

FOS GGIMviD HIIENSTIVHGOONNAM

oth

A 31iW1d

°

IP |

ne mitpeeh tea Ne Let ee 2

s, 7 ia

BisHop—Grotocy or Err Counry. 323

Quaternary Geology.

Wherever limestones are freshly uncovered in this region, their surface
is found to be polished by glacial action, the striae extending from northeast
to southwest. Excellent illustrations may be seen at Fogelsonger’s quarry at
Williamsville, in the Forest Lawn cemetery at Buffalo and at the Lehigh coal
shed near Cheektowaga. At the last named place several acres were stripped
of drift to expose the rock, which was used as the floor of the structure. The
surface was slightly undulating, well polished, with grooves rarely exceeding
half an inch in depth. One set of striae was noticed crossing the others, but
it was of limited extent and evidently of local origm. The accompanying
photograph, taken at the southern end of the shed, gives a fair idea of the
glaciation here.

Up to the base of the Hamilton group the bed-rock is covered with clays,
varying from a few inches to sixty feet in depth. The lower stratum is a
blue clay filled with smoothed and striated bowlders. Above that is a red
clay, seldom containing stones larger than a man’s fist, and at the surface is a
thin deposit of muck alluvium or stratified gravel.

A well on the farm of William P. Carr, near the lower end of Grand

Island, shows the general succession of strata, as follows :

JOrOtighy ES a a 6 feet.
ivceme emacs Sic SiS on 20“
SoibarG ele agen era ee se tk wey ti we ae DLA

A copious flow of water was struck at forty feet. The top of the well is
ten to twelve feet higher than the surface of the river, which is here twenty-
two feet deep. Another well, a mile and a half farther south, passed through
similar strata. At Sour Spring grove, on Grand Island, opposite Tonawanda,
the drift is sixty feet deep and in Tonawanda village fifty feet deep, as shown
by boring in both places. At Getzville, it ranges from twelve to sixty-nine
feet, the latter depth being found near a creek. At Rapids, a water well
forty feet deep did not reach bed-rock. Along Buffalo creek, within the city
of Buftalo, the superficial deposit is about fifty feet thick. Although the
areas outside the river and creek bottoms are more thinly covered, numerous
borings and excavations show that the average thickness of the drift over the
area under consideration is not far from twenty-five feet.

The surface of the Hamilton and Portage rocks is covered with drift
somewhat unevenly distributed but increasing in depth toward the south.
The upper rocks of the Portage group from Chaffee to Gowanda appear to

324 Report or THE Strate GEOLOGIST.

have been the dumping-ground upon which the great glacier deposited the
most of its load. In the vicinity of Zoar, the borings for gas showed, in two
wells, 825 and 379 feet of drift respectively, while the Kelly well passed
through 515 feet, which is, within my knowledge, the deepest ascertained
thickness of drift in the state. In connection with this it is interesting to
notice that the greatest depth of drift in Wyoming county, 358 feet at Gaines-
ville, is found near the top of the Portage group. Along the sides of the
streams flowing through these deposits are many thick beds of clay which
appear to be of finer quality than the great sheet which overspreads the lower
levels. These clays are often laminated, when dry splitting like shale.
Examples of these were noticed along the west branch of Cazenovia creek
above West Falls and on a branch of Cattaraugus creek near Springville.
There is also a good exposure back of the Lehigh coal shed at Cheektowaga.
Stratified sand and gravels occur in several places throughout the county,
but in no order which would indicate a general system of deposition. An
regular strip lies about midway between the limestone terrace and Tona-
wanda creek nearly all the way from Getzyille to Akron. Another extends
from Orchard Park to Elma Center and for several miles west and east of
these points. Large deposits were also noticed at Chaffee, Brant Center and
other places in the southern part of the county. While these affect the
character of the soil for agricultural purposes they are of small economic
value. The deposits utilized by railroads for ballast are usually pockets of
small extent and due to local causes. The Erie gravel pit at Alden will serve

as a good type of this class.

Soil.

The northern plain has a soil consisting largely of clay loam which
is somewhat heavy and holds water. Over large portions, however, and
especially along Tonawanda creek, there are considerable areas of deep allu-
vial river-bottom which are extremely fertile and furnish good crops. The
limestone ridge is well drained, has a larger proportion of gravel mixed with
the clay and is better adapted to wheat and other cereals. The middle plain
consists mainly of alluvial creek-bottom, well suited to market gardening
to which it is chiefly devoted. Along the lake slope south of Buffalo the dis-
integrating shale forms, with glacial gravels, a soil well adapted to fruit
raising, which is further favored by a mild, uniform climate due to the neigh
borhood of the lake. The tops of the hills southward are covered with stiff-

clay which produces good grass and supports large dairying interests. In the

VOVMOLYSSHD 'SGSHS WWOO HDIHS] ‘SO0vSdYNS MOON GSLlviIOV1y

IA 311d

é =)

ewes) =,
=o

'
Deed | , H
yy OCA hs eg

BisHop—GroLtocy or Erte Counry. 825

vicinity of Chaffee, Springville and along the slope of the Cattaraugus creek,
the deposits of glacial drift combine many elements of fertility and form a
rich and productive soil. As a whole, the agricultural interests of the county
are varied and include the principal branches suited to the climate of
this state.

Springs.

The hydraulic limestones at the foot of the Helderberg escarpment
furnish copious springs, often smelling strongly of sulphuretted hydrogen.
The largest within the county are located below the Fogelsonger quarry at
Williamsville. Within a quarter of an acre, sufficient water rises to run a
erist-mill. In searching for a source of water supply for Wilhamsville during
the past year the flow of water from these springs was measured by the
engineers and found to be one and one-half million gallons daily.

In the bed of Murder creek at Akron, just below the dam, there are
several springs, one of which fills a five-inch pipe with cold, sweet water.
Another, twelve feet away, is strongly charged with sulphuretted hydrogen.
The gas-wells at Akron, Clarence and Wilhamsville have also tapped

sulphur water.

Preglacial Erosion.

The Niagara river, as it leaves lake Erie, breaks across the lower part of
the Corniferous limestone opposite Fort Porter. The river bank meets the
lake shore bluff near the New York Central railroad bridge over the canal,
forming an obtuse angle. About a hundred yards below this bridge, between
the railroad and the canal, is a small quarry from which stone has been taken
during the past season for canal repairs. The freshly stripped surface of the
rock I found to be smoothed and striated by glacial action down to within
two feet of the bottom of the quarry, or to about the level of the canal tow-
path. Below that were evidences of glaciation but partly hidden by earth so
as to render it doubtful whether or not the striae extended lower. From the
top of the bank to the lowest well-defined striae is thirty-seven feet, eighteen
feet of which is drift, leaving nineteen feet of glaciated limestone below the
surface of the rock escarpment.

The layers next to the river were slightly terraced and the edges
afterward smoothed, showing that the rock was removed before glaciation
took place. The bed of the river opposite this place, as shown by the United
States Survey, is twenty-one feet below the surface of the river or approxi-

326 Report oF THE STATE GEOLOGIST.

mately thirty feet below the level of the canal tow-path. Across the river,
the limestone in sight is water-worn but not glaciated. The highest outcrop,
however, is not more than five feet above the mean surface of the river. It
may be assumed, therefore, that the present channel of the Niagara river at
this point existed before the glacial epoch, and was at least twenty feet below
the surface of the limestone cliff on the eastern side, and probably lower near
the middle.

Half a mile down the river on the Canadian side, near the stone church,
the water-lime is striated and smoothed by glacial action down to and beneath
the water line of the river. Photographs showing these markings and those
in the quarry on the American side are here given. It is certain, therefore,
that the present channel of the upper Niagara cannot be more recent than the
close of the glacial period, and probably was well defined to the depth of
twenty feet or more before that time.

The rate of erosion going on now is difficult to estimate, very few data
upon that point having been collected. In smaller streams flowing over the
Corniferous limestone, the amount of erosion since the glacial period amounts
to only a few inches. A view of the bed of Cayuga creek, near Bellevue, is
inserted here for the purpose of illustration. The surface of the limestone
under the bridge is glaciated on the right bank of the stream. Erosion has
proceeded through the widening of joints, partly by the action of water, and
partly through the agency of material carried along by the current. The
stream is here quite rapid when at its normal height, but the depression in
the channel shows that very little material has been removed. While the
volume of water in the Niagara river is much greater than in the stream
referred to, it is probable that erosion is there proceeding very slowly; and
that a part of the central depression, where the river now is, was excavated

before glacial time.

Preglacial Rivers.

It has been thought by Dr. Julius Pohlman and others, that a preglacial
river of large size flowed into the depression now occupied by lake Erie at
some point between the present mouth of Buffalo creek and Bay View.
This opinion was based largely upon the fact that in driving piles for the
Lehigh docks on the Tifft farm, the bed-rock was found to suddenly drop
from about thirty-seven feet to over a hundred feet below the surface. As

the rock to the northward was known to be Corniferous limestone, it was

argued that a stream of larger size than Buffalo creek was necessary to erode

alIwg 1yO4 Iv ‘30/S NVIGYNVD ‘MSAIN VYVOVIN SHL JO G38 AHL NI SONIMYVW AVIDV15

WA dLW1d

Bisuop—Grotocy or Erte County. 327

a rock of such durability to the depth shown py the excavations. Since the
matter is of considerable local interest, I have looked over the ground very
carefully for evidences of such a stream, and have collected from contractors
engaged in sinking piles, drilling and dredging, considerable data regarding
the surface of the bed-rock.

The existence of a great river at any time near the present site of
Buffalo creek or between there and Bay View is negatived by the appearance
of rock at or near the surface in the places where this supposed river must
have flowed. Stone has been quarried near Seneca and Chicago streets and
at Bailey avenue and the New York Central railroad crossing; it crops out
in the brick-yards on Clinton street near Bailey avenue, and at the end of
Clinton street. It is found near Winchester, in Cazenovia park, and in
several places between there and South park. It also is found in Smoke
creek below West Seneca. Farther away from Buffalo, the outcrops of rock
are so continuous as to preclude the possibility of a stream which, in its
upper course, did not flow over approximately the same bed as one of these
existing. At the Snow Steam Pump Works, near Buffalo creek, the limestone
was found at fifty-two feet. The wells at the Atlas Oil Refinery and the
Chemical Works touched it at about the same depth. At the upper end of
the Hamburg canal, the distance to rock is twenty-three feet, and at the lower
end twelve to fifteen feet. At the Glucose Works it was forty-two feet.
Along the Ohio basin, on the south side, the drift is from twenty-six to
thirty-seven feet deep, dipping towards the Lehigh docks. Mr. J. H. Leh
informs me that the piles were driven here six feet apart from north to south,
and that each pile had to be made a foot longer than the preceding one
to reach bottom. The southern limit of the Corniferous limestone appears to
be near these docks. At the railroad bridge across the Blackwell canal, on
the side next the lake, the piles were driven to the depth of 120 feet without
touching bottom. From the Hamburg turnpike bridge to the foot of
Michigan street along the creek and canal in the vicinity of Ganson street,
there is no rock nearer the surface than eighty or ninety feet. It is
probable that this depression is continuous with the 120-foot depth at the
railroad bridge and lies nearly at right angles with the general course of
Buffalo creek at this point.

Within a few years the United States engineers have made a series of
borings to ascertain the nature of the bottom between the southern end of the
breakwater and Stony Point. The borings were 400 feet apart and approx-

imately 1,000 feet from the shore, passing through the lacustrine deposits to

328 Report oF THE STATE GEOLOGIST.

rock-bottom. Between the end of the breakwater and a pomt opposite the
Lehigh docks, the distance from the surface of the lake to bed-rock was from
fifty-three to sixty-one feet. Sixteen hundred feet further on, the bottom was
seventy-one and one-half feet below the surface, with a mse to fifty-nine feet
within two stations. The deepest depression lies near Stony Point, where the
rock was seventy-seven feet from the surface. Beyond this the rock rises
quite abruptly, being only eleven feet from the surface at the last station near
the shore. The lake charts show a depression in the lake bottom nearly
opposite the Lehigh docks, which extends about 20,000 feet westerly into the
lake. Along this, the water is about a fathom deeper than on either side.
This depression is about 4,800 feet north of the deep depression already
referred to and, of course, more recent.

From the above facts it is probable that the preglacial Buffalo creek
entered the present lake depression between the present site of the Lehigh
docks and Stony Point, cutting its way through soft Marcellus shales between
the edge of the Corniferous and Stafford limestones.

The line where the rock suddenly drops off from thirty-seven feet to one
hundred and twenty and ninety feet, is approximately the southward con-
tinuation of the bluff seen at the Front and may have had a similar origin;
or it may be the extension of the southern limit of the Corniferous lime-
stone into the lake. At present we have not sufficient data to determine
this point.

There is no evidence to show that there ever was a great river here, or
that the drainage before or since the glacial epoch was essentially different
from that existing.

When the continent attained its present elevation at the close of the
Champlain period, Buffalo creek probably made for itself a channel not very
far from the old one, emptying into the lake near the present site of the Lehigh
docks. The sheet of glacial clays and sand, covering the valley east of the
lake to the depth of thirty to fifty feet, extended out into the lake depression,
filling the ancient channel near Stony Point to about the same depth. Across
this detritus the submerged current of the creek flowed, cutting a shallow
channel and finally losing itself im the lake beyond. Winds drifted sand
upon the beach along the lake front, forming a sand ridge higher than the
land to the eastward, like that now forming. The combined action of wind
and waves formed a bar at the mouth of the sluggish Buffalo creek, damming
it and causing it to flow northward, the sand ridge separating it from the lake

and determining its present course.

Bisuop—Gronocy or Eri County. 329

The Ancient Lake Shore Line in Buffalo.

Several deep excavations near Main street have given me, during the past
summer, an opportunity of studying the stratification of the drift in the lower
part of the city. The data collected, while mainly of local interest, throw
some light upon the location of ancient lake levels.

In the cellar of the building on the White property, above Chippewa
street, there were eight feet of sand at the surface with six feet of coarse
gravel at the bottom. Both sand and gravel were laminated, the sand
showing cross-bedding and the gravel beds sloping towards the lake. At the
Guaranty building, corner of Pearl and Church streets, borings were made to
ascertain the depth of bed-rock. According to the contractors, Messrs.
Brown & Stebell, the drill passed from the level of the curb through

toate ne oer ll... Ch or. 6 feet.

Sand and gravel to. . . . eit Coe ee ae
The cellar of the Ellicott square pcalding was excavated to the depth of
nineteen feet, and three borings were made twenty feet deeper without finding
rock. Sand to the depth of five feet was found in the corner between Main
and South Division streets, extending about two-thirds of the way to Swan
along Main, and about half-way to Washington along South Division street.
Below the sand and covering the rest of the cellar bottom was clay, the lower
part containing bowlders.

In the grade-crossing work at Main street and the Terrace, piles were
driven on the east side of Main street to the depth of thirty feet, stopping in
bowlder clay. On the opposite side of the street the piles were sunk to
twenty-four feet. At the bottom the soil was very hard, the pile yielding
only a quarter of an inch at each blow of the hammer. Near the liberty
pole, the excavation showed clean sand on the upper side, and filling of rub-
bish, brick, ete., on the lower. Here was probably the original terrace from
which the street took its name. From here to Pearl street was almost clean,
fine sand, cross-bedded and laminated, showing the action of wind. From
Pearl to West Seneca street, the bottom of the cut was through coarse
gravel showing beach action of water.

Mr. C. D. Zimmerman informs me that within the recollection of his
father the land below the Terrace was a swamp, and before the erection of
the breakwater was flooded during heavy gales, up to where the Mansion
House now stands, at the corner of Main and Exchange streets. The maps
of the United States survey give the elevation at Exchange and Main
streets as 600 feet above tide, or approximately twenty-seven feet above

330 Report oF THE Stare GEOLOGIST.
the surface of the lake. The 600-foot contour line from this point passes
through Niagara square, keeps within a block of Niagara street on the east
side as far as Maryland street, and there bends toward the lake again. It is
quite evident that the sand deposits to the eastward of this are dunes formed
by the wind, like those seen at Crystal beach, on the Canadian side, and may
have travelled some distance from the original beach. The gravel deposits
at West Seneca street and the Terrace, indicate that as an approximate
ancient shore line and go to show that the lake has not subsided more than
fifteen feet within the recent period. It is a curious fact that no shells or

animal remains are found in any of the sand or gravel beds about the city.

Modern Geologic Changes.

Mr. David F. Day informs me that old maps and prints of the vicinity
of Buffalo show islands near the head of the Niagara river between
Horse-Shoe Reef lighthouse and the site of the present breakwater. The
existence of such islands is also confirmed by the testimony of an acquaintance
of his, an old résident, who remembered seeing them. At present, their site
is marked by shoals covered by three to five feet of water. It is probable

that the wind was the most active agent in effecting their destruction.

Economic GroLoGy.
Stone Quarries.

The geologic formations which furnish stone suitable for building or
bridge work within the limits of the county, are the following :

(1) The Hydraulic lmestones.

(2) The Onondaga limestone.

(3) The Corniferous limestone.

(4) The Stafford limestone of the Marcellus beds.

(5) The Encrinal limestone of the Hamilton beds.

(6) The sandstones of the upper Portage.

The Hydraulic Limestones. The northern edge of the Corniferous lime-
stone, together with the Onondaga limestone and the underlying water-lime,
forms a more or less well-defined escarpment, extending from Buffalo through
Williamsville, Clarence and Akron to the Genesee county line. In this whole
distance there is hardly a mile in which stone has not been quarried for sale
or local use. Since the face of the escarpment shows all three formations,
they are usually quarried and sold together, so that the amount of hydraulic

and Onondaga limestone used for building purposes cannot be separately

‘@ GNY VY LY SONIMYYN AvIiOWI5

‘OWsING ‘LNOY4 SHL Ly ‘SNOLSAWIT SNOYASINYOD NI AyuvNoO

09 d¥OaNi#89 HOSEN3TIWH dOOMNAM

*.

IA SLW1d

a

P

Bispop—Gronocy or Erie County. 331

determined. At the works of the Buffalo Cement Co., at Buffalo, the over.
lying Corniferous, Onondaga, and a part of the water-lime are removed to reach
the cement stratum. The best of these strippings are sold at the quarry for
building purposes, and the company has just erected a crusher for converting
the chips and refuse into road metal. The relation of these rocks in the last-
named quarry may be seen from the following section :

Top; Flint and limestone, Corniferous, . 3 to 9 feet.
(oymeOnondaca limestone, 4... =... ...-.,-. 5° “. 8 inches.
(Se wocseamubledimestome,, ... . . .. 0." 6.4
G@yenonaleswith-cypsum crystals, . . 2. O “% 2°“
(3) Hydraulic limestone, porous, locally

knownvas oullieade «ws. To O- &
(ee Cementerock used for-buring, ... .5 “ 8 *

(1) Bottom, of impure hydraulic lmestone.

The “bullhead” stratum furnishes the greater part of the water-lime used
for building purposes. It is light chocolate to yellowish white in color, and
filled with cavities, irregular in shape, and ranging from the size of a kernel
of corn to an inch or more in diameter. On account of its porosity, water and
gases pass readily through this stone, and it is, therefore, not in favor for
cellars or similar work.

The Onondaga Limestone. This formation expands near Williamsville
into one or two lenticular masses from which it is quarried by R. & H.
Fogelsonger and J. 8. Young. Being composed almost exclusively of the
remains of corals, crinoids and mollusks, it is of exceptional purity, as is seen
from the following analysis by Hugo Carlson, of the Johnson Laboratory,

Johnstown, Pa. The specimen was from the Fogelsonger quarry.

Sangomareremmimetrs ts. Gos. Ss wc ee «964
Carbonarcolmmaenesiay. <0 6 . 2 «3s sy .*. 1.00
PERUANO OMIGe OF ION, ~ . «2 2 4 ee we es 84
pC ES OI oo a igh et ysl Be ce SAT
TUPI Pot tk ee We kt 101
JAP oes SIG THEIS | vic a aaa 017

This stone cuts easily and is used for trimmings for buildings, water-
tables, lintels, ete. A small amount is also sold for smelting purposes. The
chips and waste are burned for lime. The two quarries sold last year 260
cords of building stone and 85,000 cubic feet of dressed stone. At Fogel-
songer’s quarry the limestone has been removed to the depth of twenty feet,

and the thickness of the remaining part, as shown by drillings from a well in

332 Report OF THE STATE GEOLOGIST.

the quarry, is fifteen feet, making a total thickness of thirty-five feet. The
rock at the Young quarry is of about the same thickness.
About 150 feet north of the Fogelsonger quarry, is another known as the

“Syndicate ”

quarry, owned by Louis Wild, Joseph Mayer and Henry Smith,
of Buffalo. At present the quarry is not worked.

The Corniferous Limestone. This formation furnished the greater part
of the stone quarried within the county. The largest quarry interests are
located within the limits of the city of Buffalo, and comprise two districts.
The first includes the quarries near Main street, from the Almshouse to the
Buffalo Cement Works. These are at present idle with the exception of
the Grattan & Jennings quarry, which is selling a small quantity of stone.
The second district, locally known as “Jammerthal,” includes the region on
both sides of Fillmore avenue, from LeRoy avenue to Delavan, and extending
east along LeRoy to Worcester place, and along Delavan avenue to Dutton.
The limestone is very cherty, and on that account hard to cut, but makes a
very strong and durable building material. The layers are from twelve to
twenty-four inches thick, and blocks can be obtained of almost any desired
size. For this reason the stone is well adapted for railroad bridges, footing
for piers and for other heavy work. It is also the principal material for cellar
and foundation work for buildings of all sorts. The greater part of the stone
quarried here is used in Buffalo and by the railroads which enter this city.

Besides the quarries already mentioned, there is a small one belonging to
Cutter & Bailey near the New York Central railroad and Bailey avenue.
Another, from which a few cords have been taken during the past season, is
near the canal, just below the railroad bridge at the Front.

The greater number of quarries within the county, and outside of the
city of Buffalo, are located near the southern edge of the Corniferous outcrop.
The limestone contains less chert and is somewhat thicker bedded. The fol-
lowing section of Martin Keiffer’s quarry, near Depew, illustrates very well
the conditions which exist at that horizon. The quarry 1s situated near the

north bank of Cayuga creek.

(1), © Top, fine:sands:, <5 c24.85F 2 en 5 ee ees eenieme
(2) Alluvium containing limbs of trees,. . . . 24 “
(3) Surface of rock, rough like bed of stream,

(4). Layer of Inmesgiomes “o. ga 7h. > oan ni cee ae ee
(5). Layer of limestone te ke
(6) Layer‘of soft calcareous shale; >> = a aoe
(7) Layer of limestone, riage ere ee ome

‘ONILSVIG AS GSAOW
“QNABINIAgG YVAN ‘W33uO

au Naga
YVONAVD

SVH OQNNO8S3S4OS 13457 SHL NI WOON SHI
'ANOLSSWIT SNOYSSINYOD 3O NOISOY¥S WY JYLS

X| 3LWV'Ad

: it!
“
\,
¥
~"
t=
4
-
/*
<
a
b
;
.

Bisuop—-Grorocy or Erie Counry. 333

(Spmeaverorlimestone, = . . . «*. .-« >. 12 inches.
Comebaverotlmestome; te . % 7. i elon 4b
Chojmemecaversor limestone.) 22. 9-2). tie dd

Glacial scratches appear at the eastern end. The rest of the exposed
edge is old, roughened creek-bottom. Statistics regarding the foregoing
quarries will be found tabulated on a following page.

The Stafford Limestone. 'This rock furnishes a stone of good quality
suitable for building or bridge work. It has been quarried in the bed of
Buffalo creek at the end of Winchester avenue, below Gardenville, and at
Lancaster. The only quarry from which stone has been taken during the
past year is that of George Bingham at the latter place. No record has been
kept of the quantity, which is not considerable.

The Basal Limestone. This stone has been quarried in a small way in
the creek below the dam at Blossom. It is used there for foundations and
to some extent in the abutments of the bridge across the creek.

The Encrinal Limestone. Since this limestone consists of one or two
thick layers of a durable stone it has been quarried for culverts and abut-
ments of bridges all along the outcrop. Owing to the limited quantity in
sight at any one place, the supply has been largely exhausted except in
ravines difficult of access. The only open quarry of consequence is in the
valley of Buffalo creek, between Elma and Marilla. The quantity quarried
here was not learned.

The Portage Sandstones. Although, as has been elsewhere shown,
Portage bluestone of good quality is quarried in several places, no attempt
has been made to utilize it farther than to supply immediate local demands.
This is chiefly due to the fact, that Buffalo, the nearest market, is supplied
with durable stone from its own quarries, or gets it cheaply from a distance
by means of excellent lake and railroad facilities. In addition to the quarries
here tabulated, the following were noted which were either not in operation

or from which no statistics could be collected :

Phelps, ..*. . , . . 2 mules southwest of East Aurora.

te is 9 East of Griftins Mills.
Joseph Myers, . . «:. 2 miles east of Wales Center.
Winch 2s)... .. 14 miles southwest of. Wales.
Charles M. Brayton, . . South Wales.
Avice... . . . 4 miles north of Boston Centre.
Pike and Townsend hills, . 3 miles southwest of Boston Corners.
Daniel Sherman, . . . . 2 miles northeast of Collins.

Report oF THE STATE GEOLOGIST.

34

3

*‘qday plodod ON

*[BJIUT PROT 9YvUL OS[Y
*y10da.1 ON

“Aurenb sosta'T

‘yuasaid 4B pay1oM JON
“YAOM UNSoq Jsne

‘aae oping uo
Arend |[eus Os[e oavy

“quasaid 78 pax.oM JON

‘quesaid 4B payx10.M JON

‘[BJaut PVOA OYRUL OS[TY
“quasoid 4B payOM JON

“FG, UL Sp.lod OY A[UD

wee c cc eee es escees

OUIT[-10]VM PUB BSBPUOUG “JIUIOD

*SNOIOJIO.I09

PEEQ OSE OG OISD GOSH ow eB AAT ACO}O)

BOHR, COVSRIBSOGNOG! GOOF Gh ihraieyo)

SNOloJIUIOD

Mfela/aisiocelacreiehs 85's -SnoIOTIMION

SUTOSSOOAISESDODOO OU) Lop agai (OY)

“SnodaJLUIOD
“SnosajIUIOD
s(ajelajajevelele|n,@.>a.ejary.e.c%eia) Snoddy u109

“*SNoJoJLUIO)

“SnoIaJTM109

OGOB OOS A IOOO ISIN =|eYarehd he C07)

“"SnodajlU109

torres gnorayIqI09

DWT[-IOJVM PUR RStpUOUG JrUL0y |

OULL]-219]VM PUB LSBPUOUG "JIOLoy

SNOLOJ UO

|lnterere alela'y

SS BDLOV YOY:

yore *s**" §p10d 00S

sald SPl09 GZ

“* 86, UL SP109 0OL

“‘SMUVNAY

‘NOILVHUOY O1NOTOaY

*LNOOWYW

7" = Bp109 000°S

| sp109 090‘
|| =3*) ==" SpIOO 000g
er re) sp.09 OOF Se

Sp109 OOF T

siecle sinispsieie aia Surpling
eeense DSO OUS TS rlodijo) gare (

UWOISUOWIp puL Supping.
“UO[SMOMIp puv Surpling
“UOISHOWIpP pus Salplimg

UOIsUOIp pure Sarping

“UOISUOUILP pu SuIppmg
“UOISUOUIIP pue SuTpling
on pliq pur surpling
“UOISUDWIp pur Suipring

a iy SurtpliMg
nee nae Surpping

SanAA ELAR oe asprq
prolivs pues Supping

Surpling AAvoyy

“*"* O5pliq puv Suiplrng

‘ANOLS FO ANIY

ss" ** QUIT J[og wou “4S ULL
* goutloyueddy iou a10ul [qT
""* 9AB OIOUL[L PUR URAL
* o1OW[ [I 1vou couroyueddy
“* 9LOUl[] I trou rouroyuoddy
* gowutoyuoddy rvou a10ulyl[ LT

“youtoqueddy avwou oot [yy

“** jounequaddy wou aout
“** OLOULT[ I WOU UOISuIsudy
“ SlOU[T Ivau uOjsUIsUDy

[d t0Js0010 \\ TRAM MOJSUTSUOY

‘[d do|sooIO AA IBOU OAR LOLO'T

“{d 19js00a0 \\ Weau “OAR LOIO'T

AIOULL[L IBA WOYSUISNO y

* pRorpiRt O “A “N rvou yuo
sIOJaWAD UMT 180.10]

"8" PROLICT OLUT AOU “YS UBT

erie ete TOVOIGOE NGO ero gAdeer a)
‘MFT lou “4s gsaoqury §

“AuUVAY do NoIvooT

Stereeeseeess yoorg USN

vereess reese aEMMIORT Gee
NOW] LJ vou IauMieyueddy
Aoullaquod dy .wau a10 Ut

48 USI Sst

AERC 48 WOPSUIYSB AA EFT

OER OY AAG OLOUW] [LT 896T

> opeyng
Span adv’ Sanna oreung

aav AOLOT LLG

SERDUCODCIOOOUEDUG ONL agit
tenes SDOUGDOOCROCUOU ei) 1ft{ |

soseeseessds ULLAL JO JOOJ
‘asnoy 4WYsioly “M Y 1 'O

teen ee

OD JUoWAD oeyNng
tes sss OF qivqdsy Jeqieg
“ss ses eeee-qoRmuTaIg “seEqO
STE Foe IONS ueyseqasg
ee: Jouleaqueddy J uygor
uvUepaly FY Joyorunyos

seee ts wee

“* apulpany “H

“ Sopieg 3 Ioqyng
Whites ee eeeneres-goanaD BUEY
“""Ja0qfeqag Oo

turttsesessenee oso 1qury fT

“tee*** OF au0}g AOIA'T

soe T9sURyy

Maleiplofeltis. sie “199 “p uYyor

Ns a a *Arwyomag UABT JSo1O

OD JUEMIED puv ou0}S OjepN

n

*ssuruUuO Pr FY UBB

“SUANMQ ANY vad

‘OTVAGNA AO

ALIO ‘LONGOUd ANY SYUANMO AMUAVNO

‘WOON LNSWAD ‘GQ +xOON ,, GVSH-11NG,, O ‘S3qvHS GNV SNOLSAWIN ASOO7 ‘'X ! SNOLSSWIT VOVGNONO ‘Gg : SNOLSSWIT SNOYSSINYOD ‘VY

‘OIwsdng ‘AYYYNO LNSWSD OWsSNg NI Vlvels SHL 4O NOISSS99NS

Pe cree

"Go GYOUMYYS.1938N3 1 ¥HdOONNAM

“go sa stare

‘Cle ot 5 ee:

ss, %

X avid

3

RIE Country.

>]

Brsnop—GeEoLoGy OF

‘yeo0T | Sear a "e's QUOISpUBS OBBIIOg |*"* "~~ sp100 006 |**°"” BOBORDOR LO Rama rats pao nS apAsunds | “-9rpAsauds PgOIEOOO ss" JOSTTM “A ‘SIL
[ROOT |. RSS onomconopSD 40 --- guojspurs asnqiog Spi0o Gz cecrcrs-eesiccces Surpung [ee pe aytAsundg AOUOOM ONS altAsuadg Oe. elofBU om slevelwiaiere te sess BmIBID “WW

LR OQOUT A i aie a ae "*** 900 |spues govqlog |*****~ Sp109 00G Sa a ete iad naa J Surpling veees’ BIOINY JSBGL Cpe eee BIOINY ISB |cssteeeeeeeeeee “* SULY[UBD UBABLA(T

RR QOU EG eo eka ne OLOLSDILES aselog seess* $p109 OCT Fe hh ee popes tt ogra Suipimg “BIOIUY ISBT | ae aie aN SEER OR UR Ein fil bok TORE Re Oe yooD DO 'AA

‘[R00T sncouecodar +*252+-= gnOsaUll] PAOWBIG |--- mralelecoiaitral stele Sere Surpiing |: rerees*- ongpouey |-7° 067087 *s** IgjsuouRT |--°*° pintonatetats Sonic Sateseiele te weysuig 089
‘ormung | tedeees seresee ec seeees => SnorajIU1OD |°***"" Sp109 0C0'T | refaieserelelelalee: \sielelele\efaic!= Burpymg |v aqanuny |* ojwyng ‘4s Sinquey QGP |E aoe eae qohoW 3 ques
“[vo0'T A rail tat] Wate e S SNOIaJIMIOD FG, UL Spo CSL aan Oo ri ad aspiug | oa[[[ASuUvOIMOg | = oT [LASUBUIMOg ee lt 7 daa Y PE yg Phe m™ eMOogd seul

NL BOUT GN cuca ae Ee ed SNOJaJIUIOY) FG, Ul SP1O9 CzG Chaba ec aopugd O[[TASGBVUIMOG | ~~ ~~~" * OTA CANO So hace cae net korea TOs BB ETA ny

ord een eran eee eee cease | ance een ea teanrealns Ue Onl ste tee et PREC A cetee Ms) Bohs cart

Pa os a Cen Sain. <P abe oe SOLO FLOMOG) (hs ae ae tree LOLS LO UAT PPUe, aspiuq poorrey jot" ONAVTLeg | ~*~ A: Dip a SOLA) LOC | ODO WY selsvouveyT F snaod[[eq ‘oreyng
ROOT | wrt tesco tterceeeeeee see snoraztusog |****** sp100 009 We ourcat “-woIsuNUIp pur Surpung “peor jisuery avon | --0 ayoT oN chiovat Modoqi || 2° see. 2 sess loyary wey
S[BOON | eS ee SMOIOTULON) |r = SPLOO ONL ceeessss> JIOATNO PUB Surpling is, BoBMOYOOYGD |" USUMOIYIOYO | eel aetgs om ae Tig ce 191J9S SBLOUIIN:

pwoory |tttt ccc seeeees teres: snosagtusog |*-*** sproo oop | ttt: joayno pur Surprmng [°° + wHeMoryaayg | ts BFeMOyyoayD [ot cette esses + gasoeyy oouaIART
sroory |oveete coees eee teeees see gnogagrasog [117 spaoo got. [777 qaeAqno pur Sarpping wBvmoqyeoyg | Ss) BSeMopyaayQ octet etree ainog Ww
‘uep[y JO UMOT, i irs oe SNOLFIULOD se eee been tree ree tereeeess= > QIQATNO PUG BOPLIG LONGED TUN eee e eee wee BAOID THA [tet DORCOU ROME EOD OOS EYe At a tra (OY (
peoory [sree snosajtazog pue vSepuoug |""** sproogg ott Supping | enuag eoueanyg |e aayuag eouadelg |ine tte a werd *¢
*[ROOT dUll[-.19]BM PUB Snosa}IUI0H ‘BSeptoug . **** sp109 0OT sees oreseeeees Sarpring | SISO EOOSODS ATG NAL wees GEROOO RE GUD Coie Are ae COO CORE ODOOL OFF AFM NE} NEO) ‘MBPT H
SO[CIFNGS | sake = = OUOJSOUITT vovspuoug eS P1039) ine men Sot et ee Surpring ee oo O][TASUIBIITM | oyeyng ‘43s YBO SIZ a ae Ci hele ge OI ssunox § ‘f
‘orang | orc t ttt anoqsomy| wSepuoug ; Be po ae { veeoeeeess ang pur Surpping + gppasmrenpeay [oo opapng ‘18 RO EIgZ qaSuospaSoq “HY “UY

| | “xuuvary |
“LAME | “NOILYNYOY O1N0TOSY | “LNOOWY | ‘ANOLS JO ANIY | Seungocr | ‘ssauaay | ‘SHANMQ ANUVAY
|
‘O1VAGNA JO ALIO FHL AO ACISLAO ALNNOO AINA NI LONGOUd GNV SHYANMO XATAVAS

336 Reporr oF THE Stare GEOLOGIST.

Road Metal.

Large quantities of crushed stone are used in Buffalo by the different
companies engaged in laying asphalt pavements, concrete sidewalks and con-
crete work generally. It is used as the foundation of all asphalt pavement,
of which the city now has over 200 miles. When a stone pavement wears
out, it is, as a rule, replaced by asphalt. In this case, the old blocks, usually
of Medina sandstone, are crushed on the spot and used as the basis for the
street pavement. Chips from the Medina standstone quarries in Orleans
county are also crushed and sent in by canal so cheaply as to compete strongly
with the home product. It is, therefore, very difficult to estimate closely the
amount consumed in the city. The Corniferous limestone is generally pre-
ferred to the Medina sandstone, for the reason that it is less absorbent, both
of water and of paving material. For macadam pavement it is used entirely,
the flint furnishing a substance which is very enduring, and the limestone
serving to pack it firmly together. Neither of these materials splits readily
or breaks up under hoofs or wheels. It makes, also, excellent ballast for rail-
roads and is used for that purpose by some of the suburban electric railways.
The Buffalo, Bellevue and Lancaster railroad has a crusher at Bellevue which
furnishes ballast for that road and a large amount for surfacing the streets of
Depew. The Buffalo Cement Co. have recently erected a steam crusher with
a capacity of 450 yards a day, in which waste from their quarries, particularly
the cherty rock from the edge of the Corniferous limestone, 1s reduced to road
metal. The rock is wheeled in barrows directly to the mill, where it is
crushed, screened and loaded by chutes directly into cars for shipment with-
out further handling. The finer grades are used in concrete work, and the
coarser are sold as ballast. The Barber Asphalt Co. has the largest plant in
the city, at Fillmore avenue, near Appenheimer, where its quarries are located.
It consumes the greater part of the product, but sells some to other parties.
The Park commissioners have a crusher at the Central Park quarry, in which
road metal for the park roads is prepared. During 1895, however, they pur-
chased their supply of the Barber Asphalt Co. The Forest Lawn cemetery
has a crusher in which material for the cemetery walks and drives is prepared.
The stone is obtained from a quarry on the north side of the enclosure.

Statistics regarding road metal will be found in the following table:

'ATIASWVITIIM ‘ANYVNO S,YSONOSTSDO4 'SNOLS3INIT VOVONONO 3H

{OOGdOAMVED HOIENSTIVHOONNAM!

IXees hvala

387

a |

= |

x,

S *POATODOT UOIYBULLOJUL ON | *7 77> Spas ee pe cia ae CS are tan ole name ae alps al erie cai v earerarks| Mca stoma “"pVOI[IV1 1OySBouLTT PUv ONAS[ [OY ‘OTRYN
o *poqoore ysnf aoysnig |---- 777 77> > BECO SCORED *---"* spBor

ica} E * q 9 pue 9g910U00 ev[peq seauies LO ; ae a $e 1x “WeIp rod ‘spa “no OCF aes opegngd es aia ae ae a ie az 09D {uoume fy O[esNg
—

aS oe: cs eae ae os “pice Raa syyed pure spvor £19,000 IO |**spA “uo OQOT |>-70 TT fo Oyfainiagay [Pre eee Saeorebenoce c AI9JOMIOD UM] 4SOLO\T
“G6, UL OTON

& oe es sav 5 04, he spvor yrud roq |--sp& “no 000°9 |-*7* 77" Focal Te Yall Si opeyug |--->* ones ea SIOUOISSIMIMIOT YAIR OLLYNE

‘ Dy ey | :

3 ee ising Hee Sites (Pa Sears “a s Sper oeea SULA ALLO |= a8 pss “ON OOI0S) nea amen sp& no Q00‘O0T |-- >> opeyug [ete ete ete eects eee ee 0° Weydsy ssqaeg
8

(=) — = = = = = — SS
inal
S ‘WONNY Ud || ‘WONNY Wid

“SYUVNAY : “aS Lonaoug | ALIOVaY) “ssuuaay “SUMMOLOVADN VI

a ; |

ie) —————————— eee fo a ela ie

Fs =
ec “IVLUW GVOU AO SUNONGOUd

*
- eae ua ; \

338 XEPORT OF THE STArE GEOLOGIST.
Hydraulic Cement.

Historical, As Erie county was among the earliest producers of hydrau-
lic cement, the following facts, taken largely from “ A History of Buffalo and
Erie County, New York,” by H. Perry Smith, are of interest :

The first cement manufactured in the county was made at Wilhamsville
about the year 1825*, the quarry, kiln and mill bemg near the creek. In
1839, Jonathan Delano erected works at Falkirk, near Akron, in which he
made about 2,000 barrels of cement the first year. He furnished the cement
for the feeder dam at Tonawanda creek and for the Genesee valley canal. In
1843, the business passed into the hands of James Montgomery, who increased
the output to 10,000 barrels a year. The business afterwards came into the
possession of Enos Newman, a partner of Montgomery, and has been in his
family ever since.

In 1854, H. Cummings & Son established a cement factory at Akron,
which was operated for several years, and was succeeded in 1865 by another,
managed by his sons. This was sold to the Akron Cement Co. in 1870-71,
and the Cummings brothers erected another factory about two miles west
of Akron. Since then it has been enlarged, until now it is one of the most
complete in the state.

The first cement made in Buffalo was manufactured by Warren Granger
near Scajaquada creek, in what 1s now Forest Lawn cemetery.

Regarding this, Mr. Uriah Cummings, to whom I wrote for information,
says: “Warren Granger told me some twenty years ago that he started in
making cement in Forest Lawn just below the Main street bridge, at which
time, 1850, what is now Forest Lawn was his own farm.”

In 1874, Lewis J. Bennett began the manufacture of cement at Buffalo
Plains, near Main street. ‘The business which has been carried on continu-
ously ever since, is now in the hands of the Buffalo Cement Co., of which Mr.
Bennett and his sons are officers.

Mining and Manufacture. he stratum of water-lme burned for cement
varies in thickness from five to eight feet. It is a firm, fine-grained, compact
rock of a blue-grey color, sometimes with a yellowish tinge, and weathering to
a yellowish white. Three out of the four companies which manufacture
cement obtain the rock by mining. The method employed at the Cummings
Cement Works, at Akron, illustrates very well the process of preparing cement

for market. The stratum is here seven feet thick, cropping out on the face of

*Mr. Uriah Cummings, who has looked up the matter very carefully, gives this date as 1824.

‘OWSANG ‘ANVWdWOD LNSW3D O1VSSNG !AVLSW-GvOYN ONIMVIN HOS SHYOM

*09 OY04MV4O MOSSNI71IVH GOOMNAM

NX SLW1d

BisHop—GeroLocy or Erte Counry. 339

a high cliff some distance above the base. The cutting is made horizontally
into the rock, pillars being left to support the roof. The drills are run by
compressed air furnished by five pumps located near the mouth of the mine.
Blasting is done with black powder, trams convey the rock to the kilns, where
it is calcined and then ground by what is called the gradual reduction process.
The calcined rock is passed through four mills, being screened after each
grinding. The cement is then packed in bags and barrels for market. It is
largely used for sewers, the foundation for asphalt pavements, cellar-bottoms
and concrete work generally. This company furnished 600,000 barrels for a
single contract, the building of the new aqueduct for New York City. The
officers of the company are: President, Uriah Cummings; Vice-President, R.
P. Cummings; Treasurer and Manager, P. Cummings; Secretary, Homer 8.
Cummings.

The works of H. L. & W. C. Newman are located at Falkirk, where they
own 200 acres of cement rock. The stratum is here seven and one-half feet
thick. The rock is mined as at the Cummings works. For blasting, dyna-
mite is used instead of powder, and soft coal is used for calcining. They
make from 135,000 to 140,000 barrels yearly.

The Akron Cement Works, at Akron, have 225 acres of land adjoining
that of the Newmans, with a cement stratum eight feet thick. The rock is
obtained by mining. One of the old workings is utilized for the growing of
mushrooms, the uniform low temperature and darkness furnishing the
necessary conditions for their growth. The officers of this company are:
President, Hon. D. N. Lockwood, Buffalo: Secretary and Treasurer, Frank
S. Coit.

The Buffalo Cement Co. has its quarries on Main street, near the Belt-
line of the New York Central railroad. Blasting is done with black powder.
Since the city is rapidly extending in that direction, coke is used as fuel to
avoid objectionable smoke. The overlying rock is quarried and sold for build-
ing purposes and the refuse crushed for road-metal, thus minimizing the cost
of stripping. <A section of the rock exposed by the stripping is given else-
where. This quarry is famous for the number and excellence of crustacean
remains found in it. These occur almost exclusively in the cement stratum,
and of course are obtained only when that is being worked. Mr. Fred K.
Mixer, director of the museum of the Buffalo Society of Natural Sciences, has
prepared for me the following list of species found in the hydraulic limestones
near Buffalo, the greater number of which are from the Buffalo Cement Co.'s

quarry :

340 REPORT OF THE SrareE GEOLOGIST.

Merostomata.
Eurypteride.

Eurypterus giganteus, Pohlman.

curypterus lacustris, Hall.

EKurypterus lacustris var. robustus, Hall.
Eurypterus remipes, DeKay.

Kurypterus pachychirus, Hall.

Eurypterus DeKayi, Hall.

Eurypterus (Dolichopterus) macrochirus, Hall.
Kurypterus (Eusarcus) grandis, Grote and Pitt.

Kurypterus (Eusarcus) scorpionis, Grote and Pitt.

Prterygotide,

Pterygotus Buffaloensis, Pohlman.

Pterygotus Cummingsi, Grote and Pitt.

Pterygotus bilobus, Huxley and Salter.

Pterygotus globicaudatus, Pohlman.

Pterygotus micropthalmus, Hall.

Pterygotus quadraticaudatus, Pohlman.

Pterygotus acuticaudatus, Pohlman.

Since the last named species was described, several specimens of it im
a good state of preservation have been obtained, showing almost the entire
animal. One in the museum collection shows all but the posterior end of the
body with two-thirds of the tail. One set of antennae is preserved, and also
portions of the swimming feet. This specimen is only a foot in length, but

was probably a young animal.

Phyllocarida.
Ceratiocaride.

Ceratiocaris grandis, Pohlman (specimen nine and one-half inches wide
by five and one-quarter inches long).
Ceratiocaris acuminata, Hall.
Since the description of the last named species in the Bulletin of the
Buffalo Society of Natural Sciences, vol. 5, a specimen has been found and is

now in Mr. Mixer’s possession, which shows the shape of the carapace very —

ONINSdO BHL ONidd¥D N3SS S$! SNOLSSWIT YOVGNONO SHI ‘NOYMY 'ANVdWOD LNSW3D NOYNY SHL 3O SANIW

U2 G6 Gos MvYONOASNATIVHdOONNAM

_

IX SLWId

as
» > ier

"st

Se ra kU ee
, ae ot Le 4 t aie ee Lee =

BisHop—Grontocy or Erte Counry. 84]

well, except the pointed extremity, the eye being very clearly seen. The

body and two caudal appendages are preserved on the same slab.

Entomostraca.

Leperditia alta, Hall.

Brachiopoda.

Five forms of Discina, probably including :
Discina (ampla) grandis, Hall (¢).

Discina discus, Hall.

Lingula rectilatera, Hall.

Marine Algae.
Order FVoridea.

Chondrites graminiformis, Lesquereux.

Bythotrephis Lesquereuxi, Grote and Pitt.

The officers of the Buffalo Cement Co. are: President, Lewis J. Bennett;
Vice-President and Treasurer, P. J. Wood; Secretary, Leslie J. Bennett. The
city office is at 110 Franklin street, Buffalo.

_A statement of the interests concerned in cement manufacture is given
in the following table :

CEMENT PRODUCERS AND PRODUCT, ERIE COUNTY, N. Y.

MANUFACTURER. LOCATION. | ere | FUEL. | PRODUCT PER ANNUM.
|
5 re ees : = S st
Cummings Cement Co ....| Akron’. -....| 7 {t:........-- | Loyal Sock coal ..---.-.| 200,000 bbls.
H. L. & W.C. Newman. ..| Falkirk ...| 74 ft.......-.- [Sotticoalitsesuc.se cua: | 135,000 to 140,000 bbls.
Akron Cement Co ....-.-.. alike =| (8rft soos. - a 3 oft coallssessce esse | 140,000 bbls.
Buffalo Cement Co ....-. BudtalOe. eso mus OuN see se HCOKe SS 22 Saee cose ss | 300,000 bbls.

|

Quicklime.

The lime produced within the county is made from the Onondaga and
Corniferous limestones. From the former, lime of excellent quality 1s
burned in the kilns of R. & H. Fogelsonger, at Williamsville, and in those
of J. S. Young, about a mile northeast of that village, the product of both
being marketed together. Wood is used for fuel. aided somewhat at the

342 Report oF THE STATE GEOLOGIST.

Fogelsonger kiln by natural gas from wells on the premises. The product
marketed last year amounted to 20,000 barrels. The office of the company is
at 215 Oak street, Buffalo.

The Consumer’s Lime Co., Straub & Meyer, lessees, has three large kilns
at Gunnville, N. Y., on the West Shore railroad. The rock is obtained: from
an outcrop of the Corniferous limestone about midway between its northern
and southern boundaries. Crude petroleum from Ohio and Pennsylvania is
used for fuel, and the kilns are kept running all the year round. In 1893 the
product amounted to 80,000 barrels, the greater part of which was consumed
in Buffalo. During the present year the output has been diminished, on
account of the financial stringency which has lessened the demand for lime;
but they were unable at the office to estimate how much the product had
fallen off. The city address is 480 Hamburg street, Buffalo.

There is a small lime kiln at Harris hill, owned by A. Fiegel, which
burns lime chiefly for-local consumption. It has a capacity of one hundred
barrels in twenty-four hours, but is not kept burning all the time. The fuel
here is wood.

About half a mile north of Mill grove, at the east side of the road, is a
small kiln, owned and operated by Mr. Shaw. Lime is burned here for
neighborhood use whenever it is needed.

The preceding are all the lime kilns now in use within the county.
Remains of old kilns were noticed in several places, notably at Young’s old
quarry, northeast of Williamsville; another about a mile north of that, near
the Transit road; one east of Harris hill, on Main street, and one about two
miles north of Crittenden, on the road to Falkirk.

Brick, Tile and Fire-Proofing.

While manutacturers generally use clay as the raw material from which
to make the above products, two firms manufacture directly from shale. The
rock selected in both cases is an olive shale of the Portage group lying, in one
instance, above, and in the other instance below the lowest divisions of the
Portage sandstones. The Jewettville Pressed Brick Co. grinds the shale in a
mill. The product, having about the appearance and consistency of dry road
dust, is then pressed in moulds with a Boyd machine, which gives a pressure
of about three tons on four bricks. The firing is done in continuous, double
down-draft kilns, of which four are used. The fuel is soft coal. From 10,000
to 12,000 is the usual make per day. The total output for a year was not

learned. ‘The plant is owned by Smith & Brush.

‘OWWsING ‘ANVAWOD LNAW3SD OlvsING BHL oO SNTIy

09 dYO4 Mv4OMOTENATIVHOOMNAM

A\X 311d

Pal a
:
“SE Pe yale eee |

Bisnorp-—Gronocy or Erte Counry. 343

John Lyth & Sons, 48 West Eagle street, Buffalo, have extensive works
at Angola, in which the raw material used is shale. The rock is ground,
moistened, pressed through the dies, dried and burned in dome-shaped, down-
draft kilns. Mr. Lyth has furnished me the following statistics regarding
the product of these works from October Ist, 1894, to October Ist, 1895:

eerie ie eee he esc 389,000 pleces,
Recieinipererry Sees en) es 1. A AO7E tons.

MOU OMeKs ss. s . e ~~AT1,000 pieces.
Screener ss cer. ss. <. 8\875: tons:

PemmOgmmmr ets. =... . « » » « 652,000 pieces.
eee ee ans . : 6B00stons

The greater part of the above was marketed in Buffalo. He is now fur-
nishing material for the following large buildings which are in process of
erection: Real estate building, Pearl street ; Matthews building, Main street ;
Fuchs Bros. building, Washington street ; Buffalo General Hospital extension,
High street; Berrick building, corner Swan and Elhott streets.

The most extensive brick manufacturing interests within the county are
located in the city of Buffalo, along both sides of Clinton street, from
Scoville street to Bailey avenue, and beyond Bailey avenue in the district
included by Bailey avenue, Clinton and Ogden streets and the New York,
Lake Erie and Western railroad. The firms within these limits are F. W.
Haake and the members of the Buffalo Brick Manufacturers’ association. The
latter organization has offices at 927 Clinton street and No. 2 Builder's
Exchange. The following statement of producers, product and capacity of
works was furnished by Mr. Warren H. Brush, the secretary of the asso-

elation :

Firm. Capacity. Made in ’95.
Bcosesbtos,.. .. . . 180-M per day. 90 M per day.
iekoreovern > 2... 100“ o 80 “ «“
Georse schmidt, ..... .... 60 “ ee 60 « «
fact uebler ee. ss 60 “ ae 40 “ “

C. Berrick & Sons,-. . . 80°“ uc 20 &
Benmugleme OO. 2.» . 40“ f 30.“ «“

Total output of stock and common brick in 1895, 40,515,000.

In addition to the above, Brush Brothers have a winter plant which can
produce 30 Ma day. This will not be in operation the present winter. The

form of kiln was not noticed in all cases. Mr. Kirkover was using seven

344 Report oF THE StaTE GEOLOGIST.

Berrick kilns, and C. Berrick & Sons an equal number of Colwell kilns. As
far as noticed all were up-draft.

At Pine hill is an extensive plant under the management of Jewett &
Reynolds. In addition to common brick, they manufacture hollow brick and
tile. They have three Millington machines for common brick, one Frey-
Scheckler wire-cut machine, one Turner, Vaughn & Taylor direct-action steam
press, and a four-mould Simpson press, which is not now in use.

The South Buffalo Brick Co., H. Bender, manager, near Gardenyille, uses
a Martin brick machine, and makes about a half million of brick yearly.

The Star Brick Co., Lancaster, is workin
making two million brick, which is less than the usual amount.

The Laneaster Brick Co., office 95 Franklin street, Buffalo, has its works

near Townline. The clay bed is there thirty feet thick. The company has

g one machine this year, and

one stiff clay and three soft clay machines, the former a Frey-Scheckler. Five
of the kilns are up-draft and two down-draft. Drain tile, mostly flat sole,
with one octagon size, are produced to the number of 200,000 yearly, and
also about 500,000 hollow’ brick.

A brickyard has been started during the past summer by Mr. J. F.
Stengel on Grand Island, about a mile below the Bedell house. It is
expected to produce 3,000,000 common and stock brick per annum.

A small brickyard at East Evans, and one, owned by Mr. Charles
Seedorf, at Springville, are not now in operation.

Hall & Sons, 69 Tonawanda street, Buffalo, are the only firm making
fire-brick within the county. They consume about 4,500 tons of material,
which is brought here principally from New Jersey, with about ten per cent.

from Pennsylvania. None of the material is obtaimed within the county.

Sewer Pipe.

The Buffalo Sewer Pipe Co., at Black Rock, is the only firm manufac-
turing sewer pipe. During the past year the amount sold amounted to
600 carloads, and the increase of stock on hand over the preceding year is
estimated by the company as between fifty and one hundred carloads
more, Some clay is obtained from Tonawanda, but the larger part, with the
sand necessary to temper it, from South Amboy, N. J. The manager of this
company is Mr. N. C. Barnum.

The names of the firms engaged in the foregoing industries, with the

amount of clay products, are shown by the following summary :

VYOVMOLMSSHD ‘SOSHS HDIHS]

‘ON

10038 DNIMOHS ‘SNOLSSWIT SNOYSSINYOD SHL SO WNLVYLS Yad)

AX 411d

—

Brsnop—Gronocy or Erte Counry. 345

COMPANY. CAPACITY. BRICK. | HOoLLow Brick AND TILE.
|
Buffalo Brick Mfr’s Association.| 68,000,000 AO TOTO} OOOUSRT sR tItels eee ee oo os ee es
WSOWRRELR AKG eye's cis! caes.- 52 7,000,000 TODO LOOO™ | rh RE Soon eee eee ances te cee
{ Hollow brick, 500,000 (capacity,
Pimewe le eee sae cine see coc 4,000,000 3,000,000 <| 6 million). Tile, capacity 3
(| mill. 24 in. or 2} mill. of 6 in.
, naa sr a § | 200,000 drain tile
Laneaster Brick Co: :..<....---.-- 10,000,000 4,000,000 ) 500,000 Kaltow Wevale:
SHE TO MOG sce c5 encore shee 55 bane oeneSeeaee 25000; O00F Sew llawantesee stan See ate ieee eae Seen =
South butalovbrick Comes: —s---| 525. s-2 «2's DOOOOO NS | se come wiessmie este ea jeewieieme
| § 335,000 pieces drain tile,
DOU ay Lherdss SONS taeemact ea ce l|/=- = cece ce se gee eee ste eee ae e= 74 £0,000 pieces building brick,
( 652,000 pieces fire-proofing.
Jewettville Pressed. Brick —-:--.||.-.-..---.---. HOMOOO ton 2000p erGalys seme os sae eet ea ale ne isin = ae
Halité Sonsi (ire brick) =.= 9-0. -|\-<<2-02 =--s<< SOUND. Wee Badoetcibond -seccacb cocccoRSAS
Butfalo Sewer Pipe Co......-.--- See eee eee eee coe eee cee cee MONVOL, pipe G00) 107.00 carloads:

Sand and Gravel.

Nearly all the sand and gravel consumed in Buffalo is brought by boat
from the Canadian shore of lake Erie, near Point Abino. The dunes along
the American shore, from Michigan street to Stony Point, furnish a small
quantity, but it is not clean, and is difficult of access. Fox & Holloway,
extensive dealers in sand, estimate the amount taken from this source to be
approximately 5,000 cubic yards. The deposits at Pine hill have not yielded
much during the year. At Gowanda is a bank of sharp sand, especially
suited for mortar, which is controlled by the Buffalo Mortar and Fibre Co.
Some of the railroads have gravel banks from which they obtain ballast. The
following exhibit shows the approximate product for 1895:

PRODUCER. LOCATION OF PIT. | Propuct IN CuBic YARDS.
West Shore railroad. .--).-.22--s---.0. @laren Coc tes eee nate ene 37,112
New York, Lake Erie and Western rail-
TONG seotes coated el Se O CeO Ten ee mee Nideninace ssoae cee cece cleo e ener 29,300
IAGIIY She! Chee S5c5 Saoo see eeeeeeee Ieee Gowandaresseseee ons so oars 10,800
eit d A AE ee ee Pee Ping elle ccs as ee casas 2,000
Make Shore ® 32.2552... ee eprom a kane Near Stony, Point..-----2---5---- 5,000

346 Reporr oF THE Srare GEOLOGIST.

Natural Gas.

In this report I have endeavored to assemble all available information
regarding the development and present condition of natural gas interests in
Ene county. Recognizing the value of well records in determining the thick-
ness of geologic formations, I have taken pains to secure as many as possible.
The greater part are from the original “logs” of drillers and contractors, and,
in the main, are accurate. Where no record has been kept, or if kept, lost, the
data available have been given for what they are worth. These imperfect
records always give a gas horizon or other geologic fact worth preserving,
and usually the information of greatest economic value. With a few unim-
portant exceptions, the material included has not heretofore been published.

History. The first gas well put down in Erie county was sunk at Getz-
ville in 1858 or 1859, and is said to be still furnishing a small amount of gas.
Following the discovery of petroleum in Pennsylvania, more or less prospect-
ing was carried on in the southern part of New York, and about 1860, Oil
Creek parties secured leases in the town of Boston and drilled a well near
Patchen. This appears to have struck a fair supply of gas; but as oil was
the object sought, the gas was disregarded. About 1872 the Buffalo Gas
Light Co, put down a well at their works, near the corner of West Genesee
and Jackson streets, and struck a pocket of gas, which lasted only a short
time. Another well was drilled near Boston Corners in 1878-79, which did
not find oil or gas in paying quantities, but passed through fifty or sixty feet
of rock salt. Strange to say, the owners appear not to have understood
the importance of their discovery, for the well was abandoned. With salt
worth $1.50 or more a barrel, the well would have been a more profitable
investment than most oil wells.

The Buffalo Cement Co. made the first systematic search for gas within
the city of Buffalo in 1883, putting down a well with a diamond drill to the
depth of 451 feet 9 inches. A second well was sunk in the following year
near the first, but this also gave very little gas. A third well in 1887 gave a
good flow of gas, and was followed by several others. Encouraged by this,
in 1889, Mr. Gerhard Lang drilled a well near his brewery, at Best and Jeffer-
son streets. A fine flow of gas was found, and many other wells were
immediately started in various parts of the city. Mr. George Rochefort,
directly across Best street, got an excellent well, and the Erie County Pipe
Line was organized to take the surplus gas from the Lang and Rochefort wells
to dwellings in that vicinity. About this time Mr. Edward L. Everson struck -

a good supply of gas in a well bored in the rear of 971 Jefferson street, and,

PLATE XVI

WYNKOOP'HALLENBEGK CRAWFORDGO, ~

PORTAGE SHALES; PIPE CREEK, NEAR WEST FALLS.

Brsoop—GroLocy or Erte Counry. 347

with three others, organized the Kast Side Fuel Co. with a capital of $20,000.
The officers of this company were: President, Joseph Hottinger; Vice-
President, Albert Everson; Treasurer, Edward L. Everson. This company
was afterward absorbed by the Erie County Pipe Line organization. Shortly
after the consolidation of the two companies, Mr. W.S. Carroll, who was a
member of the Erie County Pipe Line Co., became interested in a gas well
which was sunk on the Canadian side of the Niagara river, and this well was
bought by the Pipe Line Co. As the supply of gas gave out at Best and
Jefferson streets, other Canadian wells were acquired, until the greater part of
the company’s property was on that side of the river. The striking of a
rich supply of gas in the Baker well at West Seneca, in February, 1891,
started exploration im that vicinity.

In the following year, Philip Roth and the Argue Brothers, the latter
being drillers and contractors, organized the South Buffalo Natural Gas Co.
with a capital of $300,000. The Buffalo Natural Gas Fuel Co., said to be
controlled by the Standard Oil Co., gave the South Buffalo Co. financial
backing, under arrangements mutually advantageous.

In August, 1895, the latter company had forty-five wells, three of which
would deliver 2,000,000 cubic feet of gas a day, three more that would pro-
duce 1,000,000 feet, and thirty that would produce less than 1,000,000 feet.
About the first of January, 1896, the Buffalo Natural Gas Co., which has
piped the greater part of its gas from the Pennsylvania fields, bought out the
South Buffalo Co., and now controls all the gas wells near Buffalo, including
the Canadian fields. At present it supplies fuel to about 9,000 customers.

Well Records.

Grand Island Well. (From Mr. A. B. Williams.) At Sour-Spring
grove on Grand Island, opposite Tonawanda, a well was bored a few years
ago to the depth of 3,129 feet, getting very little gas but much salt water
at the bottom. Bed rock was found here at sixty feet, the rock being
Salina shale.

Tonawanda Well. (From Mr. A. B, Willams.) At about the time
the well was bored at Sour Spring, another was sunk in the village of
Tonawanda, between the canal and the tracks of the New York, Lake Erie
and Western railroad, on the property of Mr. A. B. Williams. Bed rock was
found at fifty feet and a very little gas at 558 feet. No more gas was found
to 1,100 feet where drilling was stopped.

348 Report or THE Strate GEOLOGIST.

The Getzville Wells. (From Mr. Franklin Getz.) At Getzville, six
miles east of Tonawanda, is a group of twenty or twenty-one wells, in
eighteen of which gas was found. The best of these have a pressure of
about 200 lbs. in twenty minutes. The gas occurs at a depth of 480 to 475
feet in a soft white rock looking like gypsum. The product of these wells is
piped to Tonawanda, supplying 250 families and yielding an income of about
$7,000 a year.

Of this group, five wells are located close together near the station, and
the others scattered about within three miles to the north and west. The
drift here was twelve feet deep in the thinnest spot through which borings
were made, and sixty-nine in the thickest, the latter being near the bed of
Ellicott creek. All passed through essentially the same strata, and have
similar records, barring slight local differences of dip and location. The
following record of Well No. 17, located one mile west of the village, will
answer fairly for the whole group. It was furnished by the contractor who
drilled several of the wells, from memoranda made while the well was

being sunk.

Record of Well No. 17, Getzville, N. Y. (Received from J. H. Lichten-
burg, driller.)
Drift, 30 ye Be 2 ee A eee ee ee Bltecen
Sandvand:shale, 22 Gir sth het eee eens
White sand ‘and: shale: «) cccghetia eer eee 1 AOR
Flint shell (%), fi Oe Fa ote tke Dea Aan CCT LAO ies

Shale. gi .05 Seciyse yee ee, ee eee a ti. 2 0N tae
Salt water and! sand,-< 7 eae a ere ee G26)
Greycsandy 5025 Ce ee prema,
Siete. oc rg ee SS Se ee rae CAD (pear
Shale-and' sand: | tee ee ee eames 1-153. 1 Th
Red ‘sand, 3. Si hel ea nee “AOR (nee
Fine whitersand?s G0 eirs ane eee i 250s
Red sand and shale with sulphur gas, . .. ey oP) OSTA
Bottom :of ved. sandictG f)- ek | Bs i eee LO One
Dark sand, <j14¢. en 8: Tai Se eee bp Di Ope
Salt waterand sand). Gilechell. | aan eee Sor 28D as
Grey limestone, 1's i5. .0 20 aul i ee eee 1 300s
Salt- water-~and Sand/ss). Sain ee a tere eee LPOG o a ak

Red sand, =... «> sh 2 © See he AS BD eee

Bisnop—Groiocy or Erte Counry. 349

Flint shell Ce(exsednta): Se rhs Ie ss at 361 feet.
Syemmensamg. Aarne uk te Wee eg ee. Pe eo. Oeee
He lnckecamide Wht ene ae Sete ewe a eS crt

TEIN GSHOING ND aT SS ee oi oae
Moproenqwmiite). Gas sandisk aS ne ee LATA
Bottom of (white) gassand,... ...... Ns le

Opbonmommeyellie ainsi Se AS TAG 6
Rock much like that at the top.

The Blocher Wells, Williamsville. (From Mr. John Blocher.) These
are located on Evans street, near the eastern end of the village. Two pro-
duce gas and the other water. In boring the last the drill passed through :

MGSuGneMeeR sc Ou, a ees ie ck, 6 tor 8 feet.
Gravel and limestone alternating in beds of 8 or4 ft. to 125 “
Wry mmestones and shales to... 9. 5 2 2. 500. «
Water at 75 and 125 feet; dry all the way below.

This well was bored on the very edge of the limestone terrace, and the
beds of gravel referred to were evidently crowded into crevices in the rock.
Similar intrusion of gravel is seen in the quarry at the Front, in the city of
Buffalo. Water in this well fills a three-inch pipe two feet above the surface
of “the ground, and half fills it at six feet. It is charged with sulphuretted
hydrogen and some mineral matter.

The second well, lying about one hundred feet to the east of the one
described, struck a strong vein of sulphur gas at 500 feet. Mr. Blocher
thinks this flowed a quarter of a million feet a day on the start.

Well No. 3 is situated about 200 feet north of the others.

imethisethe distance to rodk was |... .°. 2°. 107 feet.
Maprom Niagaralimestone, "8 2 2. 101. at’ 440 4
Mopomclmion limestone, 2%) te. 00"
Maprouvtedina sandstone,...'. 2° )8'. 0 2. ° 725)
Munguebecasrsands.) AS Os et i ae
eee mene ree ion Ce er eee eT. one “S

Cased to 165 feet. Water sufficient to fill an eight-inch pipe was found
five feet above bed-rock. Twenty thousand feet of gas were found in the
Clinton, but none in the Medina. Wells Nos. 2 and 3 are now together
furnishing about 25,000 cubic feet of gas per day, most of which is used
under the boilers at the power-house of the Wilhamsville and Buffalo
Electric railway. (Record from driller, Mr. J. W. Stearns, Akron, N. Y.)

350 Reporr oF THE SrarE GEOLOGIST.

Well on the Brock Farm, Williamsville. (From H. HW. Church, driller.)
Drift 0. 3 Se ag eh not eed an an I
Shales:and limestones, ..0 2° “74.0 58> Gy oe 0 ee

Niagatia, 2 os ees oe at peeiee eare en
et i: ( ho hai eee Meee Apel oy wt
Clintons aie a pwn idly aaah aoa

ted Medina (7) via a little gas, . on Cg oe A
Shale. >" Se Sy ea ee ee eee HIG ae
First: white sands ~ 7 2° S555 Se era ere ee
Black shale es --* ¢ St mt rm ir re Sign t

White, coarse Medina neae (very fair gas producer), ie
ats Maar £00 0%
Total depth-of, welll — “2 — cates te a) ua US
Rock pressures 5,20 een ee tw ees ae

Red shale,

Mr. Church says that the red shale in which the well stopped extends

980 feet below the white Medina.

hogesonger’s Wel, Williamsville, N. Y. Samples of drillings from this
well have been arranged in a glass tube, and are in the possession of the
Buffalo Society of Natural Sciences. The following record is compiled from
an inspection of the drillings, and is based upon color and hardness as shown
by fineness of comminution, and such other characteristics as could be seen
through glass. The well was started in the Onondaga limestone, extending
from the surface to fifteen feet.
From 15— 50 feet, Bluish shale and water-lime.
50— 60 “ Brown water-lime.
60-105 “ Soft gypseous shales.

105-155 “= Soft rock, contaiming pieces of white gypsum.

155-190 “ Harder rock, light and dark chocolate color alternating

190-200 “ Grey shale.

200-210 “ Soft, light grey gypsum (7).

210-250 “ Darker, soft, gypseous shale.

250-265 “ Harder, light chocolate-colored limestone,

265-880 “ Bluish grey gypseous shale.

880-400 “ Darker gypseous shale.

400-420 “ Light-colored, soft, gypseous shale.

420-450 “ Softer, darker shales.

450-475 “ Jamestone.

Brsnorp—Grorocy or Erte Counry. 351

475-485 feet, Softer calcareous rock, with gas at 485 feet.

485-495 “ Hard brown limestone (7).

495-505 “ Soft ight brown shale.

505-540 “ Hard compact sandstone or limestone.

540-645 “ Soft limestone or calcareous shale, gas at 626 feet in
grey, medium soft limestone or shale.

645-680 “ Hard limestone.

680-720 “ Soft, hght grey gypsum (?).

720-740 “ Soft, dark blue shales.

740 “ White limestone (7) with gas.

745-760 “ Darker limestone (2).

760-785 “ Blue-grey limestone.

785-790 “ Light red sandstone (Medina).

790-805 “ Dark red sandstone (Medina).

805-810 “ Light red sandstone (Medina ?), very hard.

810-820 “ Dark red sandstone (Medina 2).

820-888 “ White, hard sandstone.

838-845 “ Grey shale (?).

845-850 “ Darker grey shale.

850-890 “ White sandstone, hard, with gas at 850. (In white
Medina ?).

890—bottom Soft red shale.

The limestone at 450-475 feet is probably Niagara.

Well at HNenmore. (Drilled by Mr. Mook; record from Miss Flora
King.) This well is located on Kenmore avenue, east of Delaware. ‘The
drill found here:

Haniel ee AS BOrteet.
Wimerilewcdter te.) ok a eat GO
(EaTUKG) TROVGISE Le are ee alae San Be SEO Dima
CIS) SUSI, «ie FN ne a le ema! 0
SENG, sc Len MES MN Si ee a 25300

} SUSU GEG.) CR al eae ee ae ea oc Drea 1" Ale
SIS, CERES eg eal Fh Pa ee oa oe ern a “ 400
Hard rock and shale, Re ee Ae re NM coer VAD
MCU Oro ne SANG, 3 ce oee wae) 4... 2, -f00 “ F265
COETS UD TRE GET Yo ORE pine eee © en ee er eee at (86:

8352 Reporr or THE State GEOLOGIS?.

Well No. 1, Clarence. (Record from J. W. Stearns, driller and con-
tractor. )

Dri: re ee ae Seer eer ee eR aire,
Salina; . <= .,... . front, d'038=465 Tectia) en eo een
Niagara limestone, “ 465-665: ©, (ee es mes
Shales.’ diss. ovvdeoeeiean 665-180.) 4 te el a ee eee
Olinton’ <3) arene 3882760. ¢ Me oe war Seen eee
Reg: Medina. i uae 160-862) (ate At eae ee Dae
White Medina, . “ 862=881 . Hi he tee i eee
Red shale to bottom of well, at 5) lags ested Shc Lae perm ey een mae

Some sulphur gas was found at 505 feet in the Niagara, and good gas in
the white Medina at 864 feet. This well is located on the east side of the
Ransom road, near the West Shore railroad tracks.

Clarence Well No, 2 is located beside the brook about thirty rods north
of Main street. It is about 880 feet deep. In July, 1895, the gage showed

400 lbs. pressure. The two wells supply thirty-five houses with gas.

The Akron Wells. There are three borings at Akron, known as the Old
Well, Well No. 1, and Well No. 2. The Old Well was put down in 1889 or
1890 in the eastern end of the village, near the Bloomingdale road. Well
No. 1 is located in the bed of the creek, about half way between Falkirk and
the West Shore railroad; and Well No, 2 is about 300 yards west of the West
Shore railroad station on the north side of the track.

The following record of Well No. 1 was furnished by Mr. J. W. Stearns:

Drift, 2 224°% 2 en Se ee ae a ee ee re ae
Salama, ig. <. oo mede, ee epdaene et oie eee eee One
Niagara,.. . «400-590: feet, 5 \..725. fey Gaacieeceeee eee ae
Shale.) B9OZ650s. “teas Gece ee
Clinton, .. << “650=685 he nee le Free ee
Red. Medina. ~-685=762:5 5-9 5) eee
W hite sande"? 762-7 Sie fae Pa Ae sca ee ae: Dae 6
Red shale, . 787-805 Cotton. coo iege eee ania Biers

All the preceding wells, together with the Almshouse and Bennett wells,

in the city of Buffalo, are located upon the rocks of the Salina group.

Natural Gas in Buffalo.
Wells ut the Almshouse, Main street, near the City line. Two wells were
sunk here to provide fuel and lights for the almshouse, one being drilled by
Mr. M. McIntyre, and the other by James Woodring. The first well was 800 —

Bisuop—GroLocy or Erie Counry. 353

feet deep, getting gas in the white Medina near the bottom, with a pressure
of 105 lbs. in thirty minutes. Well No. 2 was drilled to the depth of 1,000
feet, but struck gas at about the same level as the first, 800 feet. The two
wells are now coupled together and used to furnish heat for cooking through-
out the buildings, At first the gas was used under the boilers, running four
forty horse power and two forty-five horse power boilers; but later coal was
substituted for this purpose and gas reserved for the ranges. The original
rock-pressure was 325 lbs., and the wells are said to furnish nearly as much
gas as they did at the beginning. Information regarding the above wells was
furnished by Professor Franklin W. Barrows and Mr. Winspear, engineer at
the almshouse.

Kensington Well. This well was sunk near the railroad tracks at the
north end of the Spaulding Machine Shops. No gas was found and no record
kept of the rocks through which the drill passed.

A well was sunk for water at the Grattan & Jennings quarry, Amherst
street and Delaware, Lackawanna railroad, without finding gypsum. The

well was one hundred feet deep.

Wells of the Buffalo Cement Company. Near the Main street crossing of
the New York Central Belt-line is a group of twelve wells, eleven of which
have been drilled by the Buffalo Cement Co. Of the first three wells
Mr. Charles A. Ashburner has given an account,* which I quote:

“Well No. 1 was drilled in 1883, with a diamond drill. * * * This
well shows gas in a very limited quantity at a depth of 451 feet, 9 inches,
which slightly increased in volume down to 490 feet, 6 inches, when the
drilling ceased. The gas rock, as shown by the cores, is a very compact sand-
stone with numerous pin-point openings.

“Well No. 2 was put down in 1884 to a depth of 1,305 feet, but proved
unsatisfactory. No salt was found and but little salt water; and no per-
ceptible increase of gas was obtained beyond that shown in Well No. 1. Mr.
L. J. Bennett writes that from the best information based upon his drill-

notes, the various rocks penetrated in Well No. 2, were as follows:

Hower Helderberg limestone, . . .. . ... _. 50 feet.
Salina shales, : 5D0. “
Niagara and Clinton limestone and shales, . . . . 185 “
MWedmarsanecsomre. 2 . . a. 0 Fi. « . « 020 %

1,305 feet.”

Total,

* See ‘“ Petroleum and Natural Gas in New York State,” by C. A. Ashburner, p. 19.

23

354 Report oF THE STATE GEOLOGIS?.

In the above record the rock called * Lower Helderberg” is probably
the water-lime of the upper Salina. This well was located only six feet from
Well No. 1.

Dr. Julius Pohlman, of Buffalo, examined the samples from Well No. 2.
His record, quoted from Mr. Ashburner’s report, is as follows:

“Beginning at a spot where the rocks of the water-lime group, suitable
for the manufacture of cement, had been removed, and which is seventy feet
above the level of lake Erie, or 643 feet above tide-water, the drill encoun-
tered the following strata:

From 1— 25 feet, Shale and cement rocks in thin streaks,

25—- 380 “ Tolerably pure cement rock.

30— 48 “ Shale and cement rock in thin streaks.

43—- 47 “ Pure white gypsum.

Av— 49- < sShale:
40— (61-2 aWihte
61 1624s aepsallies

62— 66 “ White gypsum.

Pap)

yy psum.

oO
De

66— 73 “ Shale and gypsum, mottled.
73— 131 “ Drab-colored shale with several layers of white gyp-
sum, measuring eighteen feet in all.
131— 183 “ Dark-colored limestone.
133— 137 “ Shale and limestone.
137— 140 “ Dark-colored compact shale.
140— 720 “ Gypsum and shale, mottled, and in streaks.
720— 725 “ Limestone.
725--760 “-. Soft red shale.
760— 785 “ White solid quartzose sandstone, very hard.
785-1305 “ Soft red shale.

“ At 1,305 feet the drill was stopped. Permanent water was struck at
forty-three feet; gas of fair quality as well as quantity, at 452 feet; salt
water, leaving on evaporation about twelve per cent. of salt, was found at 555
feet. A shaft, twenty feet square, was sunk on the premises later, for the
purpose of determining the feasibility of mining the gypsum, but the rush of
water through the gypsum layer at forty-three to forty-seven feet, was so
strong that a pump with a capacity of 2,000 gallons per minute failed to
make any impression upon it, and the attempt was abandoned.”

Well No. 3, according to Mr. Ashburner, was 517 feet deep, striking

gas at about 460 feet. After torpedoing the well the gage showed sixty

Bisuop—Gronocy or Erte Counry. 355

pounds pressure in fifteen minutes and 142 pounds maximum rock pressure.
Six months later it gave 27,600 cubic feet in twenty-four hours, 865 feet
from the well, by meter measurement.

The other wells range from 517 to 565 feet in depth, and show essentially
the same geologic conditions as the preceding. All the wells were connected
together and the gas piped to the cement works, where it was used as fuel
under the boilers and to houses along Main street, supplying in the latter
about thirty-five fires. Mr. Bennett informs me that the gas was measured
for one season and a daily record kept of the amount consumed. The meter
showed from 58,000 to 80,000 cubic feet per day, 65,000 cubic feet being, in
his opinion, a fair average. The total amount which passed through the
meter during the season was 18,321,600 cubic feet.

The core of Well No. 1 is now in the possession of the Buffalo Society

of Natural Sciences.

The Jefferson and Best streets group. In the vicinity of Jefferson and
Best streets is a group of thirteen wells which were at one time very pro-
ductive, but are now partly filled with water and give very little gas. The
first of these was drilled in 1889 by Gerhard Lang, on his property at the
northeast corner of Jefferson and Best streets. This proving successful, he
afterwards drilled three more, two of which were good. One of these wells
supplied two boilers at his brewery for a year. After that the pressure
gradually decreased and at present all four wells are abandoned.

In the same year, Mr. George Rochefort drilled two wells on the south-
east corner of the same streets, opposite Lang’s property. These were about
1,000 feet deep. Well No. 1 furnished fuel and lights for his brewery,
running four boilers and a malt-kiln, and displacing about thirty tons of coal
a day. The gas from Well No. 2 was piped to private houses. Mr. Roche-
fort informs me that the pressure in Well No. 1 was, at the start, 525 pounds,
and in Well No. 2, 490 pounds.* At present the pressure is about seventy-
five pounds. According to Professor F. W. Barrows, one of these wells was
800 feet deep, and the other 1,100 feet.

Mr. C. Schuler, near the southwest corner of Best and Jefferson streets,
has a well which was drilled about the same time as the Rochefort wells. It
is about 1,000 feet deep and at one time yielded a fair amount of gas. At
present it is full of water and furnishes only gas enough for one house.

Four other wells were drilled on lots fronting on Jefferson, between Best
and High streets, known respectively as the Steffan, Weppner, Everson and

* A record obtained by Professor Barrows in 1890, gives pressure at that time as 200 pounds and 150 pounds.

356 Report oF THE Sratre GEOLOGIST.

Ruhl wells. Two more were located in the rear of these on an alley running
west from Berlin street. The relative location of these is shown by the
accompanying map. The Everson well, in the rear of 971 Jefferson street,
had, according to the owner, Mr. Edward L. Everson:

Drift, a a ee a Teg
Salt waters s- os). Ail Raphi: 7 commen 0) Oa ae
Gas sand (white Westie sith oo Le ae ee CEO AN 0
Well was drilledo 725". = ree: rs TOO ee

At the start the gage showed 300 a hah rock-pressure, which had
fallen, at the time of my visit, to fifty pounds. The hole is now partly full
of water which has to be removed at frequent intervals with a “Klein”
pump. Professor F. W. Barrows says of this well: “It gave a pressure of
280 pounds in twenty-five minutes, and furnished enough gas to supply
thirty or more families with fuel and lights. It was left wide open for
months, allowing the -gas to escape into the air.”

Well corner Sherman and North streets. (Drilled by Mr. Mook; record
from Professor F. W. Barrows.)

Clays yc \ Sgp nes ca Pee eee ee gree i ame eee
Lamestone, ‘Cormiferousjs .0 22 4 ee ee eee
Limestone water-lhmey=..~ 1% Yoseeon! cub feet OO
Reddish brown! water-lime, . +s. eae Wie abe Ore
Red sand and gas,o°o0 22 Gre SO ke ae
Red sand‘and gas,<@ | ska eee ee ee ee
Gas) 7a oii 4 ee a ee a ee Oe
Red shalem.)) 5 goes e220 eee es er 9G ON tote? OOM

The rock-pressure in this well was 375 pounds, the pressure running up

to 150 pounds in twelve hours.

Well at Cooks Distillery, East Side of Spring street, between Broadway
and Sycamore. (Drilled by Mr. Mock; record from Professor Barrows.)

Flint, ° ai) teal etaen pak oe ee 0 tonal Seicer
Slate and! ¢ypstm, 1m streake=..19 ig.) 520g ee Onn
Limestone,. . . <7). +.) i irom B00rorA.O0 mon s00ges
Medina sandstone; “9 cel ee eee ee
White sandstone, . . . . . . between 900 and 1,000 “

Red shale below.

Bisuorp-——Gronoay or Erte Counry. 357

No comment accompanies the above notes which were evidently given
approximately from memory. Mr. Mook thinks the well was sunk to the
Trenton at about 3,029 feet.

Well of Julius Binz, Broadway Brewery, corner Broadway and Smith
streets. (Record, approximate, from Professor Barrows. )

iiiigance hie ee tee ee) 0 fear
cdasatidemete emp. cy | wee ee ST OO Hee

NW TRIES (S ETI oS SIR ae, = ef a KO) OR aaa 2)
DOuaMcUesMaloma a Wels 7 eee er es OOO
Herdremevanocks. 9... 1 2, Bette, OOOL re

Sulphur gas was found between 600 and 700 feet. White sand with
some gas at about 950 feet, and gas in soft red shale at 1,944 feet. No
more gas was found in the well which was drilled to 2,760 feet.

The rock-pressure, in 1890, was seventy to eighty pounds in six hours,
but the gas obtained would run an eighty horse power boiler only an hour
at a time without “rest.” The well supplied twenty-two ordinary gas-
burners and the surplus was used with coal in the furnaces. The gas in this
well ceased flowing on the last day of the year 1893. At night the burners
showed the usual pressure, but on the morning of January Ist the gas had
stopped entirely and none has been produced since.

Wagner Gas Wells, Wagner Car Shops, Broadway near City line.
Two wells were put down here, the first to 1,200 feet and the second to
3,150 feet. According to Professor Barrows, Well No. 1 showed:

inedasand. wath sulphur gas. . : . ... +. at 790 feet.
Derdckewas Yeti. 2. prea eee een oe bo 1 OOO

The rock-pressure was 375 pounds at first.

Well of German-American Brewing Co., corner High and Main streets.
(From Mr. Storck, Superintendent.) This well was drilled, in 1891, to a
depth of 1,004 feet to obtain fuel for the brewery. A very little gas was found
at 800 feet, but not enough to be of use. Water at a temperature of
about 50° F., was found in abundance between 350 and 400 feet from
the top, and is used to cool the beer. The cold water takes the place of ice
and in that way has paid the cost of drilling the well.

Urban Well, on Oak street, 170 feet north of Genesee. (Drilled by
Mr. Mook. Record by Professor Barrows.) This well is 2,000 feet deep
and had a very little gas at about 1,000 feet. It is now furnishing onl)

enough for one street-lamp.

358 Report oF THE SraTeE GEOLOGIST.

Well at Water Works. (F rom Superintendent Knapp.) At 900 feet
enough gas was found to warm a house. Well was sunk to 2,020 feet
without findimg more. No record of rock passed through by the drill

was kept.

Bujfalo Gas Light Co., corner Jackson and West Genesee strects. This
well is located in the rear of the gas works near Fourth street and the
Wilkeson slip. It was bored in 1872 to see whether gas existed there, and
if so, whether this could be utilized for illuminating purposes. A small
quantity of gas was found which was used as fuel under the boilers.

Mr. Boore, the superintendent, informs me that he measured the gas for
twenty-four hours, and the meter showed 14,000 cubic feet. After ten or
twelve days the flow of gas diminished to a quantity sufficient to furnish
only one or two ordinary gas jets and the well was abandoned. The well
seems to have been of the type otf “great pressure but little gas,” as it is
said to have blown out the casing and seed-bag. The supply was not
increased by torpedoing. Some sulphur gas was found near the bottom of
the well, and water charged with some saline matter which was extremely
caustic, and irritating not only to the tongue but to the skin. Information
from Mr. Boore and Mr. Krumholz. Record of this well is in existence but

could not be found at the time of my visit.

Well in South Park. (Record from memory by Mr. G. C. Shaffer,

who was present while well was being drilled in July, 1895.)

Boi et as SO ee eee te
Shale and-limestone, . <7-. “3 .=82e-2 i SE 2S re
Bhnti@) “22 3 SS Ae eee ee eee
Limeéstone'@)) 2°. oS eee eer ee
Shale’ 120.0) .2°S ae ee ee ee
Red: Medina, \ "2" Ss 2% Stn ASR Sh ee ee Oe
Shale* "co the ape eS ee ee eee
Gas-sand, 3 ts ar Sy er ee ee
Red‘ shale) 3.) Y."205 ast a Sie shee ieee One
Red samdjo) p.0585 Pe i ee ee See
White -shale,.* \.“S.0. fui te ce eee ee Cee
Brown shale» off ees ea oh Sige ee
Red-shaley a 9) 44 oc ee a ere eee

Into. Trenton; © S.-.7>.. 2. as eee eo eee

BisHorp—Groiocy or Erte Counrry. 359

The measured distance to the top of the Trenton was 2,960 feet. The
drill passed through a part of the Marcellus at the top, Mr. Shaffer estimat-
ing it at sixty feet. Owing to the presence of the Stafford limestone so

near the Corniferous it was not easy to distinguish them apart.

Hamlin Wells, American Glucose Works, near Elk street market.
Two wells were put down here to furnish fuel and lights for the Glucose
Works. Well No. 1 was bored in 1888 or 1889, near the northeast corner of
East Market and Perry Streets, James Woodring doing the drilling. The
written record of the well and a set of samples of drillings have been lost.
Professor F. W. Barrows had access to the latter in 1890, and has fortunately
preserved the following memoranda.

42 feet, Drift.
At 42 “ Chocolate-colored limestone.
60 “ White and grey limestone.
150 “ Limestone.
650 “ Grey shale and gypsum (salt water).
Cit Sandy, with spots of iron.
726 “ Like the preceding.
800 “ Grey slaty lime.
850 “ Harder grey limestone.
905 “ Rusty red sand, chestnut color.
910 “ Same, but lighter color.
915 “ Same, but hghter color.
920 “ Same, but lighter color.
925 “ White sandstone, rusted so as to look red.
930 “ Dark red or brown, fine grains.
940 “ Light grey, rusty patches, traces of oil.
955 “ Like the last, but more rusty. (Gas.
962 “ Same, but finer grains. More gas.
967 “ Greenish grey; large grains light-grey and others dark-red,
all of a shaly appearance.
1,088 “ Dark brown shale.

The rust mentioned by Professor Barrows in several samples was
probably caused by chips from the drill oxidizing in the air. This well,
according to Professor Barrows, was 1,050 feet deep. Mr. C. Wesley, of the
Glucose Co., thought the well was 1,170 feet deep, but had no written record.

The supply of gas from this boring was very small although the rock-pressure

860 Report oF THE STaTE GEOLOGIST.

was strong. At the time of my ‘visit in November, 1885, it gave about
enough gas to supply one or two ordinary gas burners.

Well No. 2 was drilled in May, 1890, on the east side of Chicago street,
600 feet from Scott street. No gas was found here and the well was allowed
to fill up.

Well at the Buffalo Chemical Works, Abbott road and Elk street, near
Buffalo creek. (From Mr. 8. V. Fowler, superintendent, and James Wood-
ring, driller.) In 1880, a well was put down here to a depth of 250 feet
where a copious supply of water was found sufficient to fill the pipe and
flow above the surface of the ground. The water, however, was heavily
charged with sulphuretted hydrogen which unfitted it for use.

Later, wells were sunk for water at the oil refinery, a quarter of a mile
up the creek where the Atlas Works now are. ‘The same vein of water was
reached and used to cool the condensers. Large pumps were used to furnish
the great quantities necessary, drawing upon the supply so that the water
ceased to flow at the Chemical Works. The latter well was then deepened
to 1,032 feet, striking the Medina white sand. Here a small flow of gas was
obtained, sufficient for the laboratories where it has been used ever since. As
the Chemical Works were then outside the limits supplied with city gas, the
natural product was a great convenience and has paid cost in that way. The
pressure in November, 1885, was forty pounds. This well is located very
near the southern limit of the Corniferous limestone. Fifty feet of drive-pipe
were used, resting directly upon the limestone.

Well at the Snow Steam Pump Works, near Bailey avenue and the
Western New York and Pennsylvania railroad. (Record from Mr. M.
McIntyre, driller.)

,

Drifte Sse. eee eee
Limestone,and-fint,’ <2 2. S52 eon 192 feet.
Limestone and shales, changing in color, 425 “ Gliirae
Chocolate sand (limestone?), . . . .105 “ 722

Sulphur gas and a strong flow of salt
water about the middle. Water cased
off at 700 feet. Shales, dark in color,

with small shells: s\en- (feels Be See VGQr is
Red sand, varying in color from dark red
to. a: very! pale red) 2 .P-2pe) aeeea 882%

Shales and limestones, varying in eolor, 40 “ 992 .¢

“_

~~
—

Bisnop—Grontocy or Erie County. P

White sand, with gas, similar to the

white Medina, 2. . Sei feet: 937 feet.
Shales, white and red, soft- dvilling. PITMAN 987 «
~ White Medina sand, with gas, . . . . 20 “ POOR
Red shale to bottom, . . . rs, 24 O25.

‘Above record from the original au at We time of drilling.

A well was also sunk at the Atlas Works, about midway between the
last well and the Buffalo Chemical Works. No record of this was obtain-
able; but Mr. McIntyre informs me that the rocks passed through by the
drill were almost identical with those at the Snow Pump factory, so that one
record would answer for both.

There is also a well on Grey near High street, of which no recerd was
obtained. ‘The geologic conditions are said to be nearly the same as in the
Sherman-North well.

The Schislter Brewing Co., corner Emslie and Clinton streets, have a
well 1,100 feet deep. At first enough gas was obtained to hght the brewery,
but 1t has now ceased to flow. The gas horizon here was 200 feet from the

surface. Very little gas was found in the Medina.

Other Wells Outside the City of Buffalo.
Well No. 2, at Depew. (J. W. Stearns, driller.)

DNR soe edie Vow A wenitirtulyy eens, OF Leet.
Corniferous, water-lime and Salina shales, . . . . 560 “
ieee ates see ea p OT per 200K
Soe I ee oy Bde re, OO
nn See Gor Fooly | Sy ah Pee aa 80) ah
Red Medina, .. pee AP et hy ae bor ye on
White Medina (no noes apa Me turers let eed hy ered 2 yller ut
Iedushalentone 150-feett.. .. wwe . UO e164. *
Oswego sand, Cie.
Shale to top of Trenton at 2.86 Oe Cte ook tri ty one bps AS
Mirouche trenton at '3,575.feet,.- 5.5 . . . 9. >. 720%
Dark grey sandstone to 3,685, Ph) ape TOS ee PEO ae ie sere

Some gas was found at about 1,700 feet, and a little salt water in the
lowest sandstone. Well No. 1 was bored about 200 yards east of No. 2, and
had essentially the same record down to, and through the white Medina.

Both wells were started upon. the Corniferous limestone, about one and one

362 Report oF THE STaTE GEOLOGIST.

half miles from the southern limit of the outcrop. Pressure in No. 2 is
said to be 620 pounds per square inch. A company is now being formed to
pipe the gas through the village of Depew.

Alden Wells. Five wells have been sunk here, four of which are started
upon the upper part of the Marcellus shale near its junction with the
Hamilton, and the other a httle farther south upon the Hamilton shale. A
pocket of gas was found in one well sufficiently strong to lift the tools from
the well. Mr. J. W. Stearns thinks this was above the Corniferous lime-
stone. The largest supply was found in the Medina. About 100 houses
are supplied with fuel from these wells and at present there is no appre-
ciable diminution in the pressure. The following data regarding one well

were furnished by Mr. Best, who has charge of gas distribution at Alden:

Sony 0s Sy See eae Ue Nec ee ote
Slate (casing), «5 Vp ar ee wpe ceo on ee
Top of Medinay: .(j4.ui a Sealey 5 Seite neni Caen
Medima,... . 3g Se ce der oP eee
Boeket:, (s/n. iP obakt ut a Vi eee eee One

Well drilled to 1,300 feet.
The top of this well is about thirty feet below the level of the railroad

station.

Lancaster Wells. A well was sunk a few years ago on the left bank of
Cayuga creek, where it begins to widen to form lake Como. Mr. James
Payne informs me that the drill stopped in red shale at 1,850 feet. No gas
of any consequence was found. Another boring, said to be about 300 feet
deep, was made on the Lawson road about a mile south of the Como well.
A little gas was reported here, but I have not been able to verify the report.
A well was also drilled on the Borden road about eighty rods south of the
Buffalo and Lancaster electric railroad. Mr. James Woodring, who bored the
well, informs me that the well was 1,200 feet deep. The white Medina was
here but four feet thick and no gas was found. These wells are located a
little above the Stafford limestone of the Marcellus.

Well at Gardenville. July 1885.*

Marcellus shale: .. “La. Jue a ee eo eens
Limestones (Corniferous and water-lime), . . . . 205 “
Salina: shales to Niagara: /7.).0 2). hievueereane et CO

* See Report State Geologist, 1885.

Brsuop—GroLocy or Erie County. 363

A full record of this well was not obtained, the drill having penetrated
only about fifty feet into the Niagara at the time of my visit. Some gas was
found on the top of the Niagara, enough for one or two stoves, and brine

in a few feet of shale a short distance above.

Huather Baker's Well, West Seneca. ‘This is located in the village of
West Seneca, 175 yards east of the present terminus of the electric railway.
Mr. Woodring, who drilled the well, informs me that it was completed in
February, 1891. It was cased to 900 feet and was 1,133 feet deep when
finished. <A thirty-quart shot of nitro-glycerine was exploded in the gas
sand, and the pressure immediately ran up to 400 pounds in thirteen minutes,
with a maximum rock pressure of 600 pounds. The Rev. Mr. Baker informs
me that the pressure is now 375 pounds, while he is using it. The gas sup-
ples the church and school buildings, saving $3,000 a year in fuel, and also
furnishes fifty families with heat and light.

The Reed Well, located one hundred yards further east, is also a good
well, the owner claiming 600 pounds rock pressure.

Well on Eli B. Northrup’s Farm, Spring Brook. (Completed December
17, 1893.)*

PEie mene Peter etc. a) Sa 2s aephnehy ook + 0: feet,
Cer es ee fe etn ns ATA 3
TU Ree ro an Br Stat 390 >)
Wnrowwhibsrnd rocks se he yan, om DOO: wit
SyealhematiOn Bites Sie tis a eines ge eS TI OS Oke
SN GinG aNAa Rass Pt wr ok, pee ie OBS
Sig Cum Es Vesa ee so we ES OOH
ma OMpOnseeeee re os. es et 1,943 -
MOtcnae aim rneeEn cs RSs ga a we e265
bin ioe eer me O80
omote cca wn re rd tec te en, «1,308 =“
hcproime saa erst eke ees cya in) acy. 1,888. “
(MironetecamGeemenee. = a1. . . “ 1,402 “
POO mMmOrmVvelln ei sie yk alae: Ome
Well on Elbert More farm, Spring Brook. (H. H. Argue, driller.)
SSO as a eps Ua Specter ieee i la (0 17 feet.
TSIR@ SL) SERCH EDA to DORE a i ae A Ve
CCRISUTNC 0 Sk A AS es ea a

* Records marked with an asterisk were furnished by the South Buffalo Natural Gas Co

3864 Report oF THE STATE GEOLOGIST.

Shale to: flit, | "HYP ee, te Ce eee etcars
Through fhnt; .)- 2) Qe Bec So rr pee mee

Niagara limestone: * iS ey serene eet 2 oh EOS ofamee
Sulphur gas, ... 5-5 (PeMeSe i Eee ale) ee
Sulphur water, ood .:<teeeetens ue. 0, een Omen
Shale: (sixty dteet),. 0 staceeurmiies «2 teu Oey Renee ao
Clintoii, cs 5 a << gb oo, Oc) cohen sae lg

Lop of Medina; (2), \\.% 2, eee uc ++ Gece meal tonne
(ag SANG) 04) ev... ARE Ae" 2 eae aca (Om
Ce iC i ash 5 MMM ee LOTUS iL BIG Ae
Bottom-ot gas.sand (white) 5 oie. 3, 4 oi eel CO
Red srocke(800 feet) 0) et semis 9: dues eo mene ee
Black shale, 900 feet, to Bremtomy =... 2.9 = Dao LO0r nS

Well in Highteen-Mile creek, near Idlewood. (Record by Michael
McIntyre, driller.) Well started on the Hamilton shales, near the Encrinal
limestone.

Kresh waters. -. “ust are 2 ee Oe CaN
Cased out: {. (2 eee ee en
Corniterous limestone .2> 2 asa es et oes ae
Bottom/of: Cormiferous.- <2) eae A ne eee
Shale andlimestone.> -2 .. “jee eee ne ate a bO ae Oe oan
Salt water and some gas, -.) sz > sage eee yee sate Oia
Cased) Off, 0 i. Ay le ae Neca oe ee a ae) 1
Shale and limestone, saree: LOM Os aie
Small showime of gas Gn Clinton) 2.5 2 see Oar
Red. Medina, ': 2° haa ea. Garten, Bae ee GO oe Satie 0 ie
White: Medina," 207). Sac ae et ol SO Oe eee ane

The showing of gas was so small that the well was not torpedoed.
Mr. McIntyre is of the opinion that a shot of nitro-glycerine would have
made this well a fair producer. At present it furnishes about enough gas

for a grate.

Well on William J. Heiser farm, Woodlawn Beach, Hamburg town-
ship. (From Mr. Philip Lerue, contractor and driller, Titusville, Pa.)
Soil, 600.) Ws ge eee 7 feet.
Marcellus:shale; 2.8 v0.) Joe a Bi ieee le

Lime and flint, very dhard,./,.:.325 33) spelen ee eo Ue

ras
gas.

driller.

Brsuop—Grotocy oF Erm Counry.

Slate and shells to 825 feet,
Here got the “sulphur sand,”

With quite a flow of gas and some salt water.

From 733 to 1,000 feet, soft rock,
Red Medina at 1,000 feet,

Gas sand seventeen feet thick, with very little

Struck gas sand at 1,153.
Total depth of well, 1.296 feet.

Drive pipe, .
Casing,

Flint, .
Through flint, .
Niagara,
Sulphur gas,
Water and gas,

Through water and gas,

Slate,
Clinton,
Medina sand,

Through Medina eae

Gas sand,

Through gas eet

Pocket,

Well on Carl Saitz farm, West Seneca township.
1894.

Good well.)*

To flint,
Through flint,

Top of Niagara,
Bottom of Niagara,

Top of Clinton,

Bottom of Clinton

Gas sand,

Throwsli ex gas ad

Drilled,

Well on John M. Fick farm, West Seneca township.
Completed, June 2, 1894. *)

to

JY)
o>
vr

653. feet.

80) Fe
267 «
LENO ua

Stopped in red. shale.

GW ere Curtis:

26 feet.
123 (74
Balt, |
HOG
S90

1,020 «
1,060 «

1,132 “

1,200
1,223 «
1,308 “

1,326 “
ean &
1413 «

(Completed August,

366 feet.

Rete at

One
Lago) °

1242 «
1,264 «
1,360 «
1,375 «

Dp MAZE, 6

366 Report oF THE STATE GEOLOGIST.

Well on John J. Clarris farm, West Seneca township. (Drilled by H.
W. Curtis; completed December 2, 1893.)*.
Drive pipe, ".. ...://ssee Bear Se Say See eee 18 feet.
Casing,’ - 0 = 7 ae cele dee ye 2 a te)
Flint; bis." 3 See Geiger aces 2 see atwlOOr Fe
Through: flint,.: ps7 added dee {SoS Gehl ee ee OO
Niagara, lien eR geben lh: Cae ee ie eer
Sulphur gas, ..> G0 cee so. tp Pee
Ac littleswater: 8s 0s: <> .. (23m i ODO ee
More swater,” cisetie tn 4.0) eee oe S80 mee

Through iNiagaray to... -<,. (eee eee dg RO Ode
Chinton;-v- Satie eel: = ee ETL ig Dee AG:

Medina, -2 4.8) +3 (0% © 0s Re ee eee ee) erm
Through “Medimay * ar... st, (aces eee op ommend mee

Gras: sads 25 9." ay cee Rh oe ae ee ete eee ese
Through -gas-sand, .-<, 2. =. easier ars ee veel

Bottom, of; well,: ~ 2025> ccd co ee Oem:

Well on Anthony Solly farm, West Seneca township. (Drilled by H.
W. Curtis; completed September 19, 1894. Well dry.)*
Drivespipe, 34. Cet Ce = ee eee: 18 feet.

Casings) (5. Git ati 2 ae en oa
Finatyeis fa tt” ae oe ee ee ee i US Ones
Vhroueh: iit, S fu), as yo cage ee io Spa ue
Naagarays to7%5 767 Se ms Tee (2B
Sulphiir-gase-7.5.0) see es. eee OO
Waiter, tote cine. ee eae Ss eee ae 2) OlOn
Through awater. :> (cistan - abate teen sie cenee a O85. ~*#
Chlintonyarls Oh aacks. Soccer eee SAO = *
Medina, -)5-7 taco eee SasOSa. ee
Through Medina, mei 2s. 0 eee Create Om jee
Gas sald? ict.) eno pee ee ee sy ei Oe be
Through gas, sand", 2 a en ere ONS ba GE etl

Well on J. A. Timmerman farm, West Seneca township. (Stearns &
Leopold, drillers; completed April, 1894. “ Dry hole.”)*
Drive pipe, <5 .!. a Se ee 17 feet.
Casino's). 2). an ces, Oo ela gw ee
Hardt tegle: he 2, 0) op) ies aig ne ene ata 3OOH He -

Brsuor-—Grotocy oF Erte Counry. 367

ia sat ee rene Cente. ous sat | 980\ feet.
eetenGe cas. seen. tet P1100 &
Seo. eee yf oj ata Tso A
CUMMGOOEINEL “ol sn RRMEES, Cents tok cou yee, “ 1,250, “
Sieouaeen NG, SR oes oe Stes, ET OB 5%

SS OMICK Gag git fs.) oy eM lo ee! eS 1287“
Solaire a. "> 5, EM ots a ae BBD, |
SsiciOmen, <<. °. ot ed ee ti 13868.
BOuLOMMmOmmede SANG comers: oe 2 van ny SBE. “

IBOkromm@enwelln. 3 eee me x ee Sy cee 1,895 “

Well on John Schmalz farm, West Seneca township. (Completed
August 17, 1894; “Dry hole.”)*

Dee 3 FO he Se Leite ey i). D0, feet.
Casing, 4 RO. SR nee Oo,
rer, Ae els: a ate, 188°
Percale). ew el 8. te | BOO

ere) 0 eee 8, eee det CAO. ©
ee eS e.g ea oe Gee
ree ten.- a ere es op. we SS GVO M

Sie ha Er ee eg LOLS, ©
eT eS ee sb eat tn, 1.095 |
ee eo Pee sw ee LM

meen sRSAG eee ea Ale. © 1180.“
Coeme Mme ee 8 Peewee ee OE TT BG.

(Mimomeheeas sand, *) 2 nee, ee eel Sea ()Obe 4

Well on the John Sax farm, West Seneca township. (Drilled by Stearns
& Leopold.)*
ar a eee oe st. «AT feet.
ie error ee we. ys «108
RGR MOnmeIMG nye e at gk kz a Alin Mee es
ATOUOTIE TH SG Berar a C9
OM neriae wast to Lee hee ee YK B00.
Salitewanemandrsomergas ss fk et MY OTTO
GMOTOO. Senkey 2 ag RIE oy Se Se 9
LOpRGRMe le miOnin ee treet rk ot ok ot O64
Top of Medina, . ETROGOME

«

368 Report oF THE STATE GEOLOGIST.

Top*of as sand; a. 7 ce es tee Atle leo
Bottom: of ;gas sand; <2). (ere. an, Se elt oe
Bottom. of-well, ..—. -saiae eee er eee Hf lo eee

Nagle Well, West Seneca township. (Sunk January, 1895.)*
To top of flint, 9°". “Ses SS. ee teers
« ‘bottomof “lint; ~ lger eee.c6 ic 30 ae eee
top of Niagara, 20 Geos 22 <0. eee eee
bottom ot Niagaraie <<: ..) (ih seer elo nee
« top-ot Clinton,.:. ge soos |. Ge eee eee One
¢ bottom*of ‘Clinton aay... 2... >.) ) eee ee Seeger mene
« “toprol Medina, <1 Soeur oc: = ean ort el ee
“) ‘bottom: of Medina; "m2 ae? -.4 153-50 co een lee Somme:
“<top-of “gas sand, ~* yee. 5) See elo
“<“bottom of gasisand, 42 “sarin. =) .|\ bleetecnnye amen
Total depth of-well, += 3a 2 ns seen oe “

Well on Herman Metzler farm, West Seneca township. (Completed
about September 10, 1894. A good well.)*
To top -ofthint;« 42". oe en ee eee
«. bottom Of flint, 2" 35)— Re aes, Us ee ea
« “top.of Niagara, > 3. ..>\.Sacuate een) eo On
“ bottom of Niagara, = 2 Sane ee eee
«.top:of Clinton, 2» s-,.4 245) ieee eee wee el Ineo ee
* —top.of red Meédinas="".), =:.-2 So kaa ee on omer.
«bottom: of red’ Medina; “220 ¢) aac eee tI eee
Shale to top of gas sand; =< S23. = p= =. cee ele JO yan
To bottom-of gasisand, --* 2-2. 2s cea) eeu eele oto em
Depth:.of; well: :.°) G32 ce flee eee ee oom

Well on Anthony Groell farm, West Seneca township. (Drilled
September to October, 1898, by Stearns & Leopold; completed October 23,
1893.)*

Drive pipe,= i) Scie) Gackeh oe eens, aera eee 19 feet.
Casing, 01: 5 Sa Sco! AR So Bete ee ea
HWhint, 5“. <« ae oo) ae oe ev eee eS Or
Through flint, 532.) Gee Peete GS od 0iy 42
Top of Niagara; .°- <3. 6+, ao. cele ce eC
Sulphur gas,. 2° 2 bys Phage a st ove Ee

Through Niagara, |.".. 2. 0) 6. a eee

Bisuop—GroLocy or Erte Counry. 369

Slate to Clinton, - | hr a he ee at 1,070 feet.
HN et ST ee oo 2 ea a a Ct Os

ESeSN GL. . 7 eR er Ga ea Poa sls Sten ese
Minough: SisccaGes ee) edn ww 61,900

Bocuoniror well so. ONS i Sey i 1 20 Dian
Well on George Leichert farm, West Seneca township. (A. W. Curtis,
driller; completed January, 1894.)*
JOG Oe, RD aaa een 18 feet.
Cacia ee ee a. 110°
TOIT. co gt Lo ALE 0 SU heen a) re) 9

(iirouteiumang et Oe le ere es ae aro Out
Nea aS ale ee ie MOOS
SM EMEetd eee eos a ew oe ee = 9BO V4
Miirouch sulphur ast re a Ee leOGOs ©
ool hy Sa ee a Poe Melee Dam 6°
Gh filet be OS sn sale yer ao, PaO ese
iitmomonevedina, Se Soe. kG ee QOKe
Cece, SIC NE ce SE hie J AO),
Through gas Tari Cl Sie Cr aa a ae, S19 9.9 #8
Drenmomingin Welle oa ey ey Os SEO oo en

Well on Henry Hisenhart farm, West Seneca township. (Completed
February, 1895. Production in twenty-four hours, 800,000. feet).*

Mincktiesssor top sand, 1. Ae 8 80 feet,
MiiGknessor bottom Sand, 9°, 9.8.0. Ao le. og oi
Miiiekatersorespocket, aS fe Sy Bia ye

De rinomeamel ap sa tery et ea Oe. ty. 1,848., “

Roth Homestead Well No. 1. Reserve. (Thomas Argue, driller.)*
Drilled to 1,221 feet June, 1894.

Well No. 6 on Shoop farm. (Drilled by H. W. Curtis. )*

Dae DIPS ne amereee e s AG feet.
C2 eee eee. «oe B05.
RomarcommOneNIOmittee Getto 2. cw gl | TO

Cian ee ee eee lw. kl, to 1,045...
Medina, Sy rota ee As PST a i ten At, at OeOme

UO SC INGE el SS US Oe ee 0) 156, 23“
DUE CUM BaP MepeaNOy am ne a hk OBE: uM

[CUNEO UNUGE, » LOGS eS ae AP eer fe eae? sd
24

370 Report oF THE Svatre GEOLOGIST.

John Roth Homestead farm, Reserve, Well No. 1. (W. HH. Curtis,
driller.)*
Dirive- pipe; “aes 2 eee 56. feet. Dries) eee 56 feet.
Casing, 5 aed AO) OP Sinan ger tener eel
Niagara limestone,. . . at 750 “ + Cornif. and Salma, 554 \“
Through Niagaralimestone “ 980 “ Niagara,. . . . 230 “
Shales to(Gimnton, 2. 3.421.052) aSinalieg ay eer hears
Medima;' \o<.- 0.) oe oe ee 1072. = (Olio a eeene eee OMe
Through,Medina; .. >. >. —.1,160., “ (Medina. == 2 seo ome
) L168 “: AWhitesMedmar Sines
Bottomig: 0) 0s oe A ST Sed falnallen (7) ite ae aeons

Gas Sandee ics. o> 70 eG

1,181 feet.

Well No. 2 on WLS. Roth farm. (October 1894; Thomas Argue, driller.)*
Top ot @astsand:. - 2-517. he ie o--- gee tee ts
Bottom of gas sand - (4-. eee S eee L2AGs oe
Pocketee. ui. Se Ee) ee ol. ee
Total depth: Osc) 0) Sees See clezs ences

Well No. 4 on the Will Roth farm, near Reserve. (H. W. Curtis,
driller. Struck gas October 15, 1889.)*
Drivespypey 0a Sk, Sle, os Beet 0. ie OOmeer:
Casi gett 200g ony RE ee amen: 5 Te, el
Bhimnge) CSS Se cae ae at SsvnK
Flint fo 27-2 See Se Ss Se ton oom

@
Niagara, 2° Sse eho oo ee OER
Phrovgh “Niagara, <= =.) 4. iy 4 os Were eee Oommen

Slate ~70-feetto»Clintom;2 >. ee Oa F cee armel a ies
Medimay: |) 055" Sneetenhie 5k oie eek eis ~ yee aes pentane me OO ea
Ac litle asi tcc ope ua pee one aie eee ae US es eo
‘Through Medinay =) 0 tae aces ere (a VARs, nee

Gassand= 435%, aos he ot eee eee te Oneacs
Through eas sands) nese ei ee ae mit! Gn ea

‘Bottomvot- hole. <6 -3> ee eee eee ey UA ees

Schudt Well, Reserve, West Seneca township. (Drilled in October,
1894, by R. W. Argue. 200,000 cubic feet per day.)*
Top ofdiinte "5 7 0 pee eae ene at 232 feet.
Bottom of ditmt.-. fe Ga ee ear Ge mi (VG i | AY

BisHop

Top of Clinton, .

Top of Medina, .
Bottom of Medina,
Shale to top of gas sand,
Bottom of gas sand,
Pocket, .

Total depth, .

GroLtocy or Erie County.

at 1,100 feet.

“ 11380
1,210

“ 1,995
“ 1,988
60
1,298

“

“

“

4

“

“

Schneider Well, on Lot 175, West Seneca township, near Lbenezer.*
240 feet.

To top of flint,

“ bottom of flint, .

“ top of Niagara, .

“ bottom of Niagara,
“ top of Clinton,

“ top of Medina,

“ bottom of Medina, .
“ top of gas sand,

“ bottom of gas sand,
Total depth,

Goodker Well No. 1.
Top of gas sand,
Bottom of gas sand,
Pocket, .

Total depth,

Schraubh Well.
Top of gas sand,
Bottom of gas sand,
Pocket,

Total depth,

William Shaefer Well No. 1, West Seneca township.

1894.)*
To top of sand,
“bottom of sand, .
Pocket, .
Depth of well,

425

800
. 1,040
pelt)
. 1,148
. 1,228
. 1,288
1,247
. 1,802

(Drilled November, 1894.)*

“ce

“c

“

“

“

“

“a

“

“

at 1,357 feet,

“ 1370
44
ml, 414

(November, 1894.)*

“

“

“

at 1,149 feet.

1,160
: 6
. 1,166

“

cc

“

(Drilled April,

. 1,226 feet.

. 1,239

wy 1269

“

“

“

~]
bo

Report oF THE Stare GEOLOGIST.

Well No. 2, Robert Hwald farm, Ebenezer, West Seneca township.
(Completed May, 1894; 150,000 cubic feet in twenty-four hours. )*
To top.of sand,.°. 2-32 55 29 2.0 oeoS ee eer
bottom of sand.) =. fn 0” ieee eee
Pockets’) "3 02 2a eee 2 a eee Baaew
Depthtof swell, 5 (es. )s 3° at ei

Hart Well, Seneca plank road, Hast Hamburg township. (Record
from Mr. G. C. Shaffer.)
Soili tc. (eS eee er 20 feet.
Shale; -.-ueeeece ee
Bling,2 Rae. ec, ale eT CO
Liamestone(@)y8). 2. 7 Se ee eee
Slatesriic tae <a a ee ee ee) eo 60 «
Red Medina 3+"! N50 7a emma Re kee SOs

Gas*sand i se ee

Hart Well No. 5. (Completed July 1894.)*
To:tepioldirst sandio=.s “2 Sea i eles ee weer:
To: bottom: of first-sands..-—. 2.) eu oc oa ee Oe
Pocket, eo hr ae 6 eo ie Ee ee peaeame Ne
Depthuot well,“ - poxinas nore gy Eee eel ole

Hampton Well, one and one-half miles east of the Hart Well, towards
Spring Brook, on the Plank road. (Record from Mr. G. C. Shaffer.)*
Soil-and quicksand,=. JA 5 ay eee ee Otc
Shales “We! eo ar ee ee ey ee ee ee
Blntt, i oS > Sa A)
limestone,@), =<". SP h> Soa te ee ee Ome

Shale. "sar So Ge thoe oe cae eee ee A 60% 2
Red: Medina." 5a) Sei eee Sn mee
Gas Barid) 22252 ee 20S Se eee eee RYO mont

McCarthy Well No. 4, Hast Hamburg township. (Completed June,
1894.)*
To top of sand;-<\ % ¢.%~, < eeeke, 5 Sete eae Oiseau:
To bottom of Sand;.. . (.> 6 aieter a ace te ee
Pocket, eM REN Rt! ity sy eS ay Ris
Depth of well, 2° 5 a> 2 i5 (a ee eee

Brsuop—Grotocy or Erie Counry. S19

Berg Well, Hast Hamburg township. (Completed December, 1894.
1,300,000 cubic feet per diem.)*

epeGemculcande syne shar es x) 5. at 1,804 feet,

oneonnor rede Sande Pelee ae Saat CL oooes:
Shale 34 feet to top of white sand, . . . . Cleon outs
Bouwonmeor white Sand. 2.8 P)areees Ye A se LOB ine
Pocket, AR, er Bare ae De, Pye zi AAs SE
Ame U ne awl Neer ings ors cnke yeh ay ne 1,091. “

Shorr Well, Kast Hamburg township, one-half mile west of Websters
Corners. (A “6 dry hole,’?)*
DomtopeGmeagsanG. we Goh e. es gn nc {. 1,458 feet.
¢ '
ficsbouomeonerig sands =. 9.0. 2 ow. we LATE OM
Dr SHaOUCHMNOI ye yer. sie ee we ee LATS.

Well on Miles P. Briggs farm, Duels Corners, Hast Hamburg town-
ship. (Completed April 15, 1894; Thomas Argue, driller. “A rank
duster.”)*

Gye GEG InN aay oe Soa re at 650 feet.
Momo ediias:” I~ k yore ice eas Pl De layexoyee ue

PISO MICOS <. Se Peete fe ae je "Sy yy nb 623),
C1 OLE FE 10 ah ri ng re re Seu) orc’
Bottom of gas sand and well, . . ... . . se InG ious

Well on F. Boldt farm, Kast Hamburg township. (Completed April,
1894: H. W. Curtis, driller.)*
LENE s JO] VE SG SI a ig a 13 feet.
Se rie eee fk ey 3. 100:
it eee es os... Cat | 849

PMOL eee Mel. BS a ee
Niagara, tahoe geile ys EASE Sie hat co ee oN O25. 2
WASTRET > geen GW Rh ota en ae i a ea rc CEO Olu
PIO UW yaneI see ct CPS On Ae
ISLC CUO OMRON IIMGON, Seto. kw cei OA (ine
eCeNbeWnASHNG@te ee oe ee ene) penne
STRESS ie alt yaaa
(HO SENG oe ae ea rr aes tale ey wc
imonieicetasand et ke aegis e he

Prem mmormvaeliterr oe te OP eas Boe Flach 7 Oae

374 Report oF THE State GEOLOGIST.

Well on Kleis Farm, near Windom, Hamburg township. (Ma. Mook,
driller; sunk in August, 1895. Well gives about 75,000 cubic feet per day.)*
Soul: 26:6 0 dik ee ee ee ice hee ee 28 feet.

Shade. os. big eo te ep eS Ee |e) Steen
FPlimty 05 Pe ea ee

Limestones and shale to Niagara (?),. . . >. . = 640 “

Niagara ();° — 0 Ati ier 0 -. e Hl Tew et
Clinton 4.027 Adee tee os... = a eee ee

Red. Medimay=5 08 i... - pee ee
Shale: 3. 25 fee ce Se ee
White sand, Sate (0 -. . a eee ee
W. P. Roth, Well No. 1, Lot 298, West Seneca township, (H. W.
Curtis, driller; completed October 15, 1892. Gas found at 1,079 feet.)*

Casing, We Se Dal tb oe ee eh ee meets
Flint, . Seth > + hig” Re ee PWre ee licyy
Chroughsilamt icy ..) 1: <a ae eee i BASGO nk
Niawaray 25 ot LAR Se ee ean
Phrouehe Niagara’: 55257 eb. eee a 985 «
Shale 70 feet to Clinton, in Oa hee, Ee cS TOS ee
ted Medina, MEP Cr ee i te” MOTOR ae
WihitesMiedina; 3° -.0 6 es ee ee Pama ee XG pee 2
Throughiwhite Medina< <0), oy sek eee Ce cual nomen

Bottom, at PEN oo, ee Ne TER ae a rp tel al Ocoee

Dichl Well, Lot 323, West Seneca township.*
Red Medina, eae Sate tn arr ae, eee at 1,167 feet.

Gas sand... Se Sao ea ee ee Cath, Oey Oem
Through:wasisand; 27S ee eee ee Sele CC
Pocket, oe OSD peek 2 oe lg ee ee aa ‘ Oot wee

J. FH. Bassett Well, Lot 31, Hast Hamburg township, near Windom.
(Completed March 28, 1895.)*

Red Medina, Pius —e ateatan ei nan son rien tele oe eae
White Medina: =) l esc.) 2a ee ar cae Bon
Througk.savhitesMedina i: se ee ee ORES OOM

John kirtel Well, Lot 463, Hast Hamburg township. (Completed March
94, 1895.)* .
Red Medina, oo; Bite, ot bat ee See ee at 1,308 feet.
White Medina, Study del ean aie | porch foikey yeageal meee evan eae ee

Bisnorp—Grotogy or Erie County. 375
Through white Medina, ely Sit sontt yi. 1,410 feet,
Bottom of well, _ USER: Taye ise aie oe ae peters eerie ty
ROGUE euMely: < - MMMMRRD: FE BPEE epfesh i ledi ta Coch Soles 33 fle as
Titus Well, Windom. (Drilled August 28 to October 21, 1895.)*
OV ClIRN et (PR Aenea Tk, th ek ba 18h4. feet.
Lop sand iene ie ae ee hates Is) = &
Pocket, Ss lo og AAAS BY ag a ere One
Saville Well.
Dep timotmerrelinmm wr a eet TY ek 8 1502 feet.
Pocket, en tes id! iM A SS LGue
(entree snen ear et, A RT | BL

Bedford Well. (Drilled October 17 to December 38, 1895. 260,000

cubic feet per day.)*

Vel ite rn nM ron De Bdew Maine es th BBO feet.
Pocket, MMII RE i kag Ae. Sow at
Top sand, PPM SEES oe Sed ley) Oy

Beaver Well, Hbenezer. (1,208 feet deep; good well.)*

Kast Aurora village. A well was drilled here between May and
October, 1893, to the depth of 1,800 feet. It is located near the railroad
“tracks about 200 yards south of Main street. A very little gas was found,
and also brine which produced, upon evaporation, twenty per cent. of salt.
The depth at which they were struck was not ascertained.

About two miles southwest of East Aurora, on Cazenovia creek, a well

was sunk in the eighties, of which the following is a partial record : +

Shales (Lower Portage Hamilton and Marcellus), . 695 feet.
Corniterous limestone (and water-lime?), . . . . 165 “
irom me above: imestones to salt,-9 29... 605 CM

Saturated brine was found at 1,465 feet, filling the well and running
over the top. The stratum in which the brine occurs was reported to be
seventy feet thick. No attempt was made to utilize the brine, and the well
is now abandoned. At one time considerable gas is said to have escaped
from this boring, but at the time of my visit, in August, 1895, the amount
would barely support one ordinary gas jet. Surface gas in quantities suth-
cient to burn, bubbles up from crevices in the bed of the creek in several
places near by, and I suppose that the gas found in the well was from the

same source, the black shales of the Portage group.

+ See Report State Geologist (N. Y.), 1885.

376 Report oF THE STATE GEOLOGIST.

Half a mile further up the same creek a well was drilled for oil, about
the year 1875. No record of this is preserved, but it is reported that gas
was found at 900 feet, with sufficient pressure to throw water over the top
of the derrick.

Well at Pipe Creek, near West Falls, This well was put down in
1865, to the depth of about 1,000 feet. Mr. A. L. Henshaw, who furnished
me these facts, says that the pressure at first was sixty pounds. The
well is now full of water from which the gas bubbles up vigorously, furnish-
ing about a cubic foot a minute. Another shallower well was bored a little
further up the creek, but struck no gas. Surface gas escapes from fissures
in the bed of the creek in several places. One crack furnishes enough for

four or five gas-burners.

The Colden Well. (Record by Mr. A. H. Hayes.) This well is located
one-fourth mile south of the village, on the west side of the creek. It was
put down by a stock company of which Mr. Hayes was an officer. Gas was
found at 800 or 400 feet in sufficient quantity, as Ma. Hayes thinks, to supply
the village with fuel. From the description of the flow, it appears that the
well must have been a good one, but the gas was allowed to go to waste.
Here, also, there is much surface gas. A water well fifty feet deep, in the
village, furnishes enough gas to keep a street-lamp going all the time.

Another well, on the hill between Colden and Boston, was bored about
the time the Colden well was sunk. Mr. A. L. Henshaw visited this while
drillimg was in progress and saw the gas burning, From his description I

should judge the flow was not large.

Wells at Patchen, Boston township. ‘Two wells are located here, one
in the village near the creek a short distance south of the bridge, and the
other some fifty rods further up the creek. Mr, John H. Wait, who worked
upon the well while it was being drilled, furnishes me the following
information :

Well No. 1 was sunk on the Wait farm, to the depth of 762 feet, by a
company from Oil Creek, Pa. about the year 1860. A strong vein of gas
was found at 272 feet, which escaped with such force as to stop drilling for
three days. The pressure is described as sufficient to lift two men seated
upon the ends of a plank laid across the top of the casing.

Later on another company, from Oil Creek, leased farms in this vicinity
and put down well No. 2. At 320 feet they struck gas, but the flow was not

so strong as in well No 1. At 940 feet they struck a hard rock (the

oo
a
a |

GroLtocy or Erte Counry.

Brsnor

Corniferous 4?) which proved so difficult to drill that the well was abandoned
at 1,000 feet. This well still gives a blaze two or three feet Ingh when
ignited. Near the old well is a spring which gives off gas all the time.
Six other gas springs are also reported from the town of Boston.

The Old Boston Well. This is located on the Henry Jones farm on
the east side of the creek three or four miles south of Boston Corners.
Mr. H. N. Drake of Findlay, Ohio, has kindly furnished me the following
information regarding it:

“In 1878 or 1879, Mr. Chubbuck and myself took the contract to sink
the well to the depth of 2,000 feet. For the first 1,000 feet the rock was

black shale contaiming some gas. At 1,225 feet we struck a very hard rock

.

which we called flint and limestone |Corniferous 7]. At about 1,800 feet
we got rock-salt about sixty or eighty feet thick, some of which was clear as
crystal and some dark in color. The rest of the rock was a sort of rotten
sand. At 2,008 feet we struck a vein of mineral water that colored the tools
and cable black as ink and had a very disagreeable odor. The depth of the
hole was 2,140 feet. There was no sign of oil from top to bottom.”
The record of this well is very interesting for the reason that the
presence of rock-salt seems to have been discovered here at about the time
it was found in Wyoming county, a fact not heretofore published. The
horizon of the Corniferous limestone is distinctly defined, and quite
probably the water charged with sulphuretted hydrogen was the vein often

found in the Niagara elsewhere in Erie county.

Well at Kden Valley. (From Mr. Daniel Schweickhart.) This well is
located about a mile east of the village and about thirty feet higher than the
railroad station. The well was sunk by Mr. Schweickhart previous to
1884, to obtain water for his brewery. The record given from memory at

the time was as follows: *

i ee rere. lf. «Cf | «CLD feet.
Pir tenner ee. |e. . «61 200
iiowlle elljiey 0» LSS = Se RO le Sn ace 0
RtieiiMc aIGucHnGOW tec ste. wl. ©4400
PER TSCURELOCMM treet er ys ke te | DO

LOT “
This well has since been deepened and furnishes enough gas for his

house and brewery.

* See’ Report State Geologist for 1885

378 Report oF THE SvarE GEOLOGIST.

Angola Wel. (About 670 feet A. T.) This well is located upon the
farm of Mr. Alvin Eddy, three-quarters of a mile south of Angola on the
road to Brant Centre. No record of the well is preserved, but Mr. Eddy
gives me the following facts from memory :

Struck rock, 32 ja Bae Ghee ie ee el eet
Limestone (Connmeroug))) o>... =e ae Si) Osa
Through limestone (?), a hard rock here, .. aril kOe
Well drilled Swe... ee tonlea00 25

Some gas was found near the bottom of the well. At present the hole
is full of water and gives very little gas.

Mr. J. R. Newton of Angola has a well 450 feet deep on his premises.
It is said to furnish sufficient gas to heat his house.

Well at Kenton, near Brant. (Drilled in 1890 and 1891.) The original
record of this well is lost. The following facts are furnished by Mr. Clarence

M. Fenton, who had charge of the work of drilling the well.

Soulrand, quicksand) ts iia Si eer 80. feet.
Hard ‘blue rock; 7) a5) Ra ee oe ee Ome aa
Vein-ot waiter =. 2 tact Ae Ce eee at; 1.300;-%
Red sand with good flow of gas, .. tt OO One
Drilled o's AER yp ce ET ne eae so ane toeleae

The well was torpedoed with 100 quarts of nitro-glycerine and filled with
packer and two-inch piping. When confined the gas pressure runs up to
1,000 pounds to the square inch. When blown off, the well furnishes only
vas enough to fill a three-quarter inch pipe, or about 10,000 feet per day.
This is used to run the cappers of the Erie County Preserving Co.’s cannery
at Fenton, and supplies also two or three stoves. At present the well is
three-fourths full of water heavily charged with salt.

While drilling was in progress a greasy rock was found at 1,200 feet,
from which there was a flow of gas sufficient to make a flame two feet above
the top of the well. At the same time the cable was smeared with a dirty

mixture of tar and yaseline, smelling of petroleum.

Wells at Zoar.
Kelley Well, three-quarters of a mile west of Town line. (Completed

January 10, 1888; record from Mr. Michael McIntyre, driller.)
Drive pipes: ni. "Us. ek wie Pee eee 60 feet.
Gagne oo 8 wo wT ge Se ASR Ne eal i ea ee ee (

Top of Corniferous limestone, 4) +.) eee Ons

Bishop—Grorocy oF Erte County. 379

Hirstoulcareem) and gas: 9. 720. A Oe >... 1,725 feet.
Second oil (amber), with salt water, .

]
homme ruonie) eee ee ee 1,825). -

Kerr Well. (Begun August, 1888; record from M. McIntyre. )

Drivwenpipe.( Chroust) 5s. Ve + 879) feet.
ret cmeehs Oe IC nok kee eS GBR
Toy OT ACCTING, SE ke ee es ie OY G25 a
Gas, eo ee Pea se 88h“
Depchroimwmelvammmrpee a ce Te eR ele 2,150“

This is the largest producing gas well yet found in the county, and
probably in the state. Gas was struck on October 27th. There was, at the
time, in the well, the string of tools sixty-five feet long, together with more
than 1,800 feet of rope, the whole weighing probably two tons. The escaping
gas forced everything out of the well and at least 150 feet into the air, The
drill, in descending, struck upon its end and penetrated the soil to the depth
of fifteen or twenty feet, bending the stem lke a wire. The noise made by
the gas escaping through a five-inch hole could be distinctly heard at Spring-
ville, nearly six miles away. It was ten days before the pressure decreased
enough to permit the resumption of drilling, and Mr. McIntyre estimates that
during this time the daily flow could not have been less than twenty-five or
thirty million cubic feet. The well is now owned by the Buffalo Natural
Gas Fuel Co., and is known as the “ Freak.” Ordinarily it is held in reserve,
the pressure gradually rising to about 600 pounds. When an unusual
amount of gas is needed, this gas is turned on to the line, and the well furnishes
a million feet a day for a period of two or three weeks. By this time the
pressure has fallen to about 300 pounds, and the well is shut off and allowed
to “rest.” In the course of two or three weeks the pressure rises again to 600
pounds, and the well is re-opened.

The horizon in which this gas occurs is probably the upper part of the
water-lime, the rock immediately below the Corniferous limestone.

Along the northern outcrop of this rock in Erie county, there is a layer,
locally known as “ bull-head,” which is filled with cavities from the size of a
pea up to several inches in diameter. This rock also contains cavernous
seams through which subterranean waters flow and appear at the outcrop in
copious springs.

The immense volume of gas from the Kerr well indicates that the gas
accumulates in a cavity so large that it cannot readily empty itself when

opened,

380 Report oF THE STavTeE GEOLOGIST.

Richardson Well, near Mortons Corners; Lot 92, Collins township.
(Begun March 5, 1889; M. McIntyre, driller.)
Drift, 5 'C:, lorie eg eee cP aa 80 feet.
Casimgy 2°02) CAST ein A ec ee oh ieee

Top. of :Corniferous.” “=>... eee eee
b]

Smallishow: ob-casies ete 7 "0 oe ee (eNO eee
Salt “water te y aeeen bd en re Ar 2eO Ou wee
Salt water, chocolate-colored sand, . . . . OS oir
Through limestone and shale, . . . .. . Pee Oil eae
Red: Median 20). eee ee ee CONDE yy mee
ThrovghoMedina,. (5 in) ee een ee CDDEO 3 yn ae
Limestone and shale to white Medina, . . . HD iy ies us
Throughswhite: Medinaus (Sitti tpane eee al: LODO Mma

Redeshialle.:\- -.<! at Pneba | e eee Be ct ti DO, OO Onaaes
To: bottom. 9.5 42S Oe, er eee Ome

Well on Monroe Kelley farm, Zoar, one-half mile west of Kerr Well.
(From Mr. Michael McIntyre.) This well showed the greatest thickness of

drift known to me in the state, namely, 515 feet.

White Well, Zoar. (Completed July 2, 1892; record by M. McIntyre ;
controlled by the Standard. )
Drive pipe; at go oe ns ee te, een el HO encots
Casings s/o gS We eo a ake eee ea eee ee
Top-ot ‘Cornitérous, ~ 2 i ob ee ee OS le
First 88.0 0 See es a ee Serene AO
Second gas; [2 . « 2a) pone ceaee eens een) ae

Depth of well ~ 2 .-. 0. “ape aia i een eC

White Well, No. 3, is 800 feet east of the Kelley Well. White No. 1 is
600 feet east of No. 8. White No. 2 is 1,400 feet east of Well No.1. Of
these No. 1 1s the best well.

White Well, No. 1, Zoar flats. (Record by Mr. M. McIntyre.)
Drive pipe, 0p) oe seal eae eee een eee eticars

Top of Corniferous," 2) > Seer ee eee leo Onn

Hirst gas.) 15 sae Se aie SE ees Ona
Second sos. y) 600) m0 Ges eee eee ee OO OM ms

Depth of well, <2). f:0.u.°) Soa nat uke ete eg

Bisoorp-—GroLocy or Erie Counry. 381

Frye Well, Zour. (Record by Mr. M. McIntyre; 100,000 cubic feet daily.)
iniceipe mmr in i se reeay ie ee ae >. 165 feet.
at ee eee eee) er ks £65
WOnMnreh OMe meee 5 a eee enir. Alt A BS hs cab 1.570, «4
ADRESS esata’: SMe et Ge tre, Seale apy
Mecondnomse(WESU) 5 Sj ymumale: 4 fe- 6 ale ts elkopo.
lire acer ot eh Me oe aN es ara)
De Viineet ace Pee nD OO)

White Well, No.2, Zoar flats. (Record by Mr. M. McIntyre. Top of
well 20 feet lower than Well No. 1, which is 1,400 feet away.)
Dri neem oo, Se or - LGD: feet.
Cant RP re Sa oy eee ecw. OBO

iopror Cormmerous, 6 Be ke aAuaieoGO 2%
sat Jimmie ts 5. | Ss Si aa ge GOO) t
VitiGhrsaliawaheR mere 5 =. 2, ato Se ks oO.

EMORMGUOMCH, MMC i ae OOO

Parkinson Well, top of hill, Zoar. (Record by Mr. M. McIntyre.)
This well furnishes about 25,000 cubic feet of gas daily.
Dreamer. «. Sees is Oo ws | BOB feet.
Cae ie ren ee a ee te es cytes) ABR, -&
Memo ornilerous, sewe( iy. ey oS. oy Hat 1,720.“
DOME OmORS: 0: Re gue wn S| ey Paleade. 1
inGueommOimmelly "= Malena, le ae 2.001. «

The last well sunk at Zoar, September—October, 1895, is situated about
2,000 feet south of the Parkinson well. It had—
Dritteeeemrnte tc ret 4. ee | 60 feet.
CqenicroUss meee ses ta ee at 1 445 OC
Plein. ers. ea net i to 1809 «

Well on the south side of Cattaraugus creck, opposite Zoar. (Record from
Mr. M. McIntyre; no gas worth piping.)
Pie ee Set ye ts. 80. feet.
er eer erent ire ce, a fiw iini ce. 2. APO. &
NOprOlC GPMMLGrOUS N Pagcce ee oc). ke aonb (OOspas
BOM OMONeaMOVCHS tees of 865, =
Wemulegumwellpea wer er ees. ew ao te oe L,950-

382 Report oF THE STATE GEOLOGIST.

A part of the gas from the Zoar field is piped into Springville, where
it supplies about 120 families. The company controlling it is called the
Springville Natural Gas Co., of which the officers are: Dr. Brooks, president ;
H. Leland, treasurer; F. D. Smith, secretary. There is also a board of

directors, of which Mr. M. McIntyre is a member.

The Springville Well. (From Mr. Mook, driller; well contains twenty-
five feet of rock salt.)

Blue sandstone and shales, . . . . . =. - .~. 1,800 feet.
Jatestomes. <3. Qa es, eee tie ee ere
Salts cubs cae 1, Cees oo" 2) a a at 1252574
Well ibored. 2 see ea" 5.) 2. 2 See eee ee bow? boUN IE

At Gowanda, on the Cattaraugus county side of the creek, a well was

sunk, in the eighties, by Mr. Silas Vinton, who gave to me the following

record :
*Sonle hae se eo, ee 6 feet.
Shale, — -ee a. “6 Aa ee en Ot
Sand; withvoull’and: gas) c=.) es ee :
Shale to “second sand,” where more oil and gas
were found. 22. ~~ (a5 SS Gee ee ee eee
Shale. -32c3-<65° see ee ee ee eo ee
Hard rock (Corniferous and water-lime), . . . . 400 “

1,700 feet.

Mr. Charles 8. Howland informs me that this well was deepened in
February, 1889. The Corniferous limestone was reached at 1,390 feet.
Drilling was continued to 2,251 feet, where salt water and mud were found
and the well abandoned. The well, when cleaned of water, gives gas
enough to fill a two-nch pipe with a light pressure. This well is located
near the creek, about 200 yards east of the station.

Another well was drilled over thirty years ago on the Erie county side
of the creek within the village limits. Locally it is known as the “Trunk
Well.” Gas was found at about 860 feet, and the well was drilled about
forty feet deeper. This furnished gas for a house for several years, but is now
“filled up with a substance resembling glass and nearly as hard.”

* Vide Report State Geologist 1885.

BrsHorp—Groniocy or Erie Coun'ry. 883

Maps.

The location of gas wells and gas territory is shown upon the general
map accompanying this report. Where the scale was too small to show
details accurately, enlargements of the more important districts have been
given. The map of the South Buffalo field was constructed mainly from data
furnished by Messrs. E..M. Cobb, President, and C. T. Sloan, Vice-President
of the South Buffalo Natural Gas Co.. who have allowed me the free use of
their maps and the original records of wells drilled under their direction. In
this map, wells known to furnish little or no gas are marked (*). Those
which were bemg drilled at the time the information was being collected are
marked (+). Wells marked ({) are either good producing wells now or were
at some time. The names, location by lot number, and the character of the

wells are shown on the following table designed to accompany the map.

Name of Well. Lot. Township.

Samuel Wasson. 28... .). = . . 85° West Seneca.

ecley sc ee Pe. LOD is a #
OAV anispeKomnme AF 2 ies > geo 12 « fs f
Brel hveas, ok a> pe OR Rese os, oy, SLED ee “ %
idee eerie MOUremmR Re oe er oa A : “ 4
Mee chnerderNnt ne 5 lu a ari g LA Ms ig t
iieenezer Station, §/.00) 2. <0...) o. °189 “ a +
Olly, Ser Se eee ey en Sa #
Pa nemwnAnkeren sted. o. os) oY ce . 288 a ; t
INGE. | Re ana RS eee a ee Tf E ‘ af
eWepplem Nor. Gh ws oa. ij) 296 c ss if
Soe No <P ie Gir eo 7298 ¢ ci if
Sussm@ssenvat, PALO. oe B89 Mé es t
AV DoOtnwemeem tas le eons eso B46 a ts 33
Pediord «oan treat 859 a a if
Low NUCL .. 9 Simmer eS BB F a s: 1
ot arose ss Wem a, ol tes. B86 « sg if
Sconce onevery. Ti make meet. .c >? . 840 « ee :
Cree Pichia us, Ln As, sa +. 898 a fe t
OMe nwaler moPn tse &.e ey ci: s; 2. 329 a g t
Johan scmudte. Bk ys x 3. 880 a ef ds
Gepo@lamicnn te sieette Vo. :.. .864. ‘ és t
PEM CREO CARA Py es sa. ke gue, OOS a“ as "i

384 Report OF THE State GEOLOGIST.

Name of Well. Lot. Township.
C.Schudt, .°'.. . 78 Sie ee OTS essence nee
Herman. Metzler". =. 4 eee oe z a
J. Nagel tus |. oo eens ee on ea) “ r ;
George-Reichert,. = S22 ge os | Sac eee E fF
H. Grotke, 3° 493 Se aaa ose ae * +
J. Timmerman. pee ee. see es : t

439-4 é
G. Reichert: (vient 2c eed < f He
William Schaefer, ee | Orie ee eS at a t
EH, ‘Hisenivarts elves ee. 5 eee oo oe fe se
J; Picks Roepe: 335: 7) eee eles co ¢ d:
W ilhame CsGrotke. <5. a eee el o cs t

9Q3 “ “ %*

IQA “ “ t

370 “ “ if

168 “ ce i
Blogsome i. 300s bt ee ee ee ae *
Biions: Vala (Sates! tr Ae epee OO 3 t
Elma Station, . Shes OD Me AN
Springbrook (Albert Moore), . . . 81 A it
Bi Rottw oR ee eee 91 f eS
G:Schimalz:- =)": Set Ler ke e

448 East Hamburg. *

400 « «“ +
CO. Spawer, f) 25) bei eee On € és +
J. Sehwartz, ch >*:- eA ee ee F gf t
Oarl, Betas 26 SUR ae ee a is if
Timothy McCarthy, . . GN Ss s t
Duell’s Corners (M. P. Briggs), . . —— # a
F. Boldt; ~ 4°. 277oier Sia eee oS us t
G. Seitz, 2 krete ete 460 ge es if

463 a S ai
Alfred Moore, =5y ti Dalia ate ell bee EO sf t
Bassett,... . 6. =p AS ae ee z =
W..K, Saville;siicic ete eee 2 . af
John Johnson, ol Sees? col ate ce ewes 17 ‘ S *
Henry J; Hart a... gta’ cla ee eee i at t

Brshorp—Gro.tocy or Erte County. 385

Name of Well. Lot. Township.
Meatthas Senor) fo. |. . 2; . & 21, Hast Hamburg.
Eee ria pton, So Meee conse ee 1d e bs
Pedal dl. DOnZIe!: vt ce ex ese) 26 s iy
Ruin H-holmwoode. -. -. :.- 64. ~“ i
ler ost... teen a, 3D: + Hambure. t
inom. an. Ss em Ses) 2 yt D2 t
12 Shere end RR” 7 a a i AE ae t

Wells Outside of Erie County.

The following well records are interesting in connection with the

preceding :

Well No. 1, Philip Zavitz farm, located on Lot 35, third concession
from lake Erie, township of Bertie, near the town line of Humberston,
Ontario, Can. (Record from Mr. E. Coste.)

plete we Teen Sw fe 7 feet.
SoLnnerous 0-7: > Wil Aa Uomieet erie” yolk Se *
Onondaga shale, gypsum

dolomites (Salina pd.),to . 415 feet, . . . 390
Guelph and Niagara, . . 415-655 “ ee eel f

Wimetare-shale- 3. . ..,. 655-705. “ i ae
Clinton limestone, . . . 705-735 “ tat ome rel) ne.
Medina sand and red shale, 735-846 “ =f ee a

Gas in white Medina, . . . at 836 “ esang.. «13. “* thick

At Point Abino gas was found at 500 and 575 feet below the surface, or
193 feet below the bottom of the Niagara limestone.

Well No. 1, Corfu, Genesee county, N. Y.; north of the village. (From
Mr. J. W. Stearns.)

Marcchussisle: 2) wee nt wee eS | O80 feet.
SMC wera ee) oar tack eee ee | | 180
inestoveraniustialcms. 02. ean fe S.C. (488
PePeMesEONem eo ee... Cw 250
ee tea eee eee ae se! TO
Clinton, a te AE 0 al 10
*Medina, Par eee cos A L100“

inedepmale co potromofiwel,... . . . . - . + 20 *

* Notes say ‘‘ white Medina.”

25

386 Reporr oF THE STare GEOLOGIS?.

Well No. 1 on the Bradshaw farm, near Coomer P. O., District 13, Lot 36,
town of Newfane, Niagara county, N. Y. (Record from Mr. E. Coste.)
Well begun in red shales of the Medina group.
Trenton; '.-? .9 2 pabell4eb eet:
Continued? 5 3 to GQ aldara 3! aes eee Cr
Caleiferous sandrodlke to .2sL25 = “(7 a. 2 eee ee eh (oe
Laurentian: Vee. aie 105
Drilled: into: Laurentian 21. 6 See ee a)
Depth of well, . .~ ~s 234 feet.
Well No 2 (drilled January 4, 1892; started on the red Medina. Record
from Mr. E. Coste.)
Drive Pipe, :22 see es eg ee eee ele
ted Medina, dark Hudson river and Utica
shales," 0s “SBP ome O00 cleets
Trenton, “2.0 a Se 0S OO Sees wih Obama
Calciferous;. --~<.° ~ eo 1980s eo te ame
Hydromica and dark green schists of the Archean,
from. 2225 Age LO s0S98 0) teet. sneer oN Ore
No Potsdam sandstone was recognized. This well had a little gas, from
1,912 to 1,918 feet. Cased to 243 feet, and was dry after that.
Record of Well at Fulton, N. Y. (Mr. J. W. Stearns, driller.)
Drrtts 38) See ee ee ee 43 feet.
ned. sand, — 48, 2k eC oe rae eee Ree CeO Oram
(A little gas at 320 and 370 feet.)
Oswego grey limestone, 72." 578. strom 690i ton 150 710

Sand and limestone, Eee OO Maae

Limestone’and: shale. <4) 3. 0. = eee SEU NO ae
Black -shalé,+ >, * 2. -.5= ipego> is) Soe ee el toa iet
Lop: of Trenton, 3.8 ate ene eee come Omar

Gass. eos we FES ee ee ee Sl eae ho cles
Gras, . os uacind ees ce ee Om

Gras, cathy OMe aa es a
Gas, aul. ht Gt Se ee eee ‘POO aes aly
Drilled’: sf 5° cis cle pa Saat ee ani eso q

A well in the village of Canandaigua, N. Y., has fifty-one feet of rock
salt, according to Mr. James Woodring, of Buffalo, who sunk the well.
A well was also put down on the Indian Reservation at Versailles, N. Y.,

to the depth of 216 feet. No gas was found, but good water was obtained.

BrsHop—Gerotocy oF Erte Country. 387

Surface Gas.

Small quantities of gas escape from crevices in the rocks in many places
within the county. The most abundant supply comes from the Portage rocks
in the horizon of the lowest sandstones along a line connecting roughly
Wales Centre, East Aurora, North Boston and North Collins, and extending
eight or ten miles southeasterly. The lower Portage shales also furnish
supplies from rock crevices and water wells, and the Hamilton and Marcellus
some from similar sources.

A few of the points at which gas has been noticed are at Highteen-Mile
creek, near the lake; between Wales Centre and East Aurora, where the
town-line road crosses a brook; near Holland; in Cazenovia creek, between
East Aurora and Griftin’s Mills; on Pipe creek, near West Falls; in many
places in the town of Boston; in the ravine between Shirley and North

Collins and near Lawton’s station.

Gas Horizons.

In the wells which have penetrated the Trenton limestone in Erie
county, no gas has been found. The Bradshaw well, No. 2, in Niagara
county, however, furnished a little in that rock. The Depew well. No. 2,
struck a paying streak of gas in the red shale, a little less than 1,700 feet
below the top of the Corniferous limestone. Nearly all the gas obtained
within the limits of Erie county comes from the “ white Medina” sandstone,
although some is found in the higher “red Medina,” and occasionally in the
Clinton. The gas obtained from these sources 1s comparatively free from
sulphur and makes excellent fuel and a fair illuminant.

The upper part of the Niagara group furnishes a variable amount of gas
in many of the wells throughout the field. The most characteristic con-
stituent of this gas is sulphuretted hydrogen (HS), commonly known
as “sulphur gas.” Water in contact with the gas dissolves out the U,S,
becoming “sulphur water.” Hence sulphur gas and sulphur water may occur
either together or separately, and the presence of either in the same formation
may determine the gas horizon. In ten wells it was found at depths varying
from 25 to 172 feet below the top of the Niagara, two having it at about
fifty feet and three at 130 feet. In six wells the average distance was 130
feet, which may be assumed as the horizon where we would be most likely to
find it.

Wells No. 1, No. 2 and No. 3, at the Buffalo Cement Works, struck gas
at 450 to 460 feet, or about 400 to 410 feet below the Water-lime. Allowing

388 Report oF THE Strate GEOLOGIST.

386 feet for the Salina shales, this gas horizon would be fourteen to twenty-
four feet below the top of the Niagara. Getzville well No. 17 struck some gas
at 265 feet, which was unquestionably in the Salina shales; but the greater
part was found at 474-481 feet. The record indicates Niagara at 361 feet
or 292 feet from the surface of bed rock. The gas horizon was 113 feet
lower and was undoubtedly in the Niagara.

In connection with this it is interesting to examine the record of the
Boston well. Rock-salt was found here 575 feet below the top of the
Corniferous or a probable distance of 407 feet below the water-lime. At
783 feet below the top of the Corniferous, or 615 feet below the water-lime, a
vein of water was found, evidently sulphur water, which was very offensive
and colored the drill and cables black. As the Salina shales are thickest
in the trough containing the deposit of rock-salt, it is apparent that the
drill in this well had penetrated some distance into the Niagara lime-
stone. The Corniferous limestone and water-lime appear to act as the
reservoir for gas in the Zoar field. In three wells quite a show of gas was
found within ten feet below the top of the Corniferous, one had gas at forty-
five feet, and two others at seventy and eighty-five feet respectively. Three
had gas between 100 and 130 feet, and the famous Kerr well found it at 160
feet below the top of the Corniferous. Although a cavity was undoubtedly
the reservoir in the last imstance, the porous “bull-head” of the water-lime
is the most probable receptacle for gas within the formations named.

A pocket of gas with a flow sufficiently strong to throw the tools out of
the well was found in one of the wells at Alden. The reservoir was in the
Marcellus and was quickly exhausted. Shallow wells in the Portage rocks

furnish small quantities of gas in a few instances which are elsewhere noted.

Natural Gas Reservoirs.

The geologic conditions controlling the accumulation of natural gas are
not sufficiently understood to furnish reliable data by which a gas well
may be located. There are no surface indications of anticlines or other results
of deep-seated disturbances which might act to accumulate and hold large
quantities of gas. In the Medina sandstone, which is here the principal
reservoir, the gas is found where the rock is soft and porous, but is not found
where the rock is hard. Whether this difference in hardness is due to flexure
of strata or to some inherent quality of the rock itself, 1s still to be deter-

mined. Good wells are found close by poor ones, and several “dry” wells

Bishop—GeroLocy oF Eri County. 889

may almost encircle a good one. The most experienced and intelligent men
in the gas business frankly say that the drill is the only means of ascertaining
whether gas exists in the earth or not. And after a careful study of the
conditions existing in Western New York, I am free to express the opinion
that the presence of gas in any locality in Erie county can not be predicted as
securely as, for instance, a salt-well might be located in Wyoming or Living:
ston counties. In localities already tested, the chances may be two out of
three that a new well will find a paying quantity of gas. In a new district
the first well might get it, or it might not be found by sinking five or six.
The wells put down during the past year, however, go to show that natural
gas is much more widely distributed than was at first supposed, and that it is
destined to wider use, both for fuel and lights. The greater part of the best
wells are located along the Marcellus outcrop or on the Hamilton shales, just
south of it; but it is extremely doubtful whether proximity to the outcrop
has anything to do with the production of the gas.

It has been shown that surface gas exists in considerable quantities in
the Portage shales. Although the supply from this source may not be suffi-
cient to pipe to a distance, it appears to me that this might be utilized for
local consumption. A well from 100 to 500 feet deep, if properly located,
might furnish fuel for several houses; and it is by no means impossible that
the time will come when a gas well in that region will be considered as

necessary as a water well.

A General Geologic Section of Western New York, from Lake Ontario
to Cattaraugus Creek.

By using the well-records from Niagara county, in connection with those
from Erie county, the approximate thickness of the several formations is
shown from the Archean, up to near the top of the Portage group. Since
the measurements have been obtained from drillers’ records, lithologic
characteristics, such as hardness, color and material have in most cases

furnished the data by which the formations are distinguished.

The Portage Group, m the Boston well was 938 feet thick ;

in the Zoar wells 1,346, 1,895, 1,490; and in the Richardson well, 1,541 feet.
The Genesee shale, at Eighteen-Mile creek, was seventeen

feet thick, but is thicker eastward. At Windom it is estimated,

Wwitnoeut-actualmenasurement,to be wc. 2 fk 25 feet.

390 Report oF THE STaTE GEOLOGIST.

The Hamilton and Marcellus shales in the well at Eighteen-
Mile creek are, together, 287 feet thick. In the Heiser well at
Woodlawn, one and one-half miles north of the edge of the
Hamilton, the Marcellus is 125 feet thick, and is probably not
less than 140 feet in all, making the Hamilton shales,
and the Marcellus shales,

The Corniferous limestone, Onondaga limestone and

Water-lime, all being hard, are classed together by drillers as
“flint.” The well at the Snow Steam Pump Works, near the
southern edge of the Corniferous, in Buffalo, had 140 feet of this
flint. The Sherman-North street well had 150 feet. An examin-
ation of twelve other wells gives an average of 168 feet. The
wells at the Bennett cement quarries, Buffalo, begun below the
Onondaga, had, with the cement and “ bull-head” lying above the
mouth of the well, sixty-two feet of water-lime. The Fogelsonger
well on the same horizon had sixty-two feet of hard water-lime,
thus giving of
Corniferous and Onondaga limestone, —.

Water-lime, .

The Salina shales, from the bottom of the flint to the hard
rock known to drillers as Niagara limestone (but eae includ-
ing some Salina), averaged in ten wells,

Making the Salina and Water-lime together 446 er ae

The Niagara includes an upper limestone and a shale below,
the latter averaging seventy-two feet in thickness. The whole in

ten wells averaged .

The Clinton was from twenty-three to forty feet thick, and

averaged in nine wells,

The Medina, mcluding (@) a hard red sandstone, the “red
Medina;” (4) a shale of varying thickness, sometimes absent
entirely, and (¢) an almost white siliceous sandstone, known as
“white Medina.” These collectively ran from 83 to 140 feet in
thickness, the white band being from four to thirty feet, but
usually ten to fifteen feet thick.

Nineteen wells gave, of the whole, an average of

147 feet.
140 feet.

108 feet.
60 feet.

386 feet.

319 feet.

27 feet.

109 feet.

Bispop—-GroLtocy or Erie Counry. 391

From bottom of white Medina to the top of the Trenton lime-
stone, the Albert Moore well gave 1,635 feet; the South Park
moleee00 feceucand the Depew well 2... . 2. . . .. » 1,869 feet.

The Trenton limestone in the Bradshaw well, near lake
Ontario, was 680 feet; in Well No. 2, 710 feet, and in the Depew
lr Ue wk eC. C20 feet.

The Calciferous, resting on the Laurentian gneiss, was in the
Bradshaw well, No. 1, ten feet; in No. 2, twenty feet; in the

Depew well, 11¢ feet.

Without reaching the Archean, total thickness of above section, 5,561 feet.

The deep Richardson well at Zoar, which has been quoted

above, passed through the white Medina at . . . .. . . . 2,910 feet.
Adding from the Depew well, the shales below, . . . . . . 1,869 “
reid: hes mentees fy tases Scie bois alias cee « 720
Wicich) Calciememnmmrning Gera i toil iiah Warsieujd thse eerie ace oe . 110 &
Nea werumEmneOh en ett ee ws ts 5,609 feet.

A difference of only forty-eight feet in the results, as shown by the two
computations, shows that the estimates are approximately correct. It will be
noted, however, that the Calciferous was not fully penetrated in the Depew
well, and that the Richardson well 1s not situated upon the highest land in
that part of the county; so that the total thickness 1s probably from 100 to

200 feet more than the result given above.

Rock-Salt.

The borings in Erie county have added materially to our knowledge of
the extent of the Western New York salt-field. Thick beds of rock-salt are
known to occur at Boston Corners and at Springville, while the northern
edge of the same deposit was pierced in the old well southwest of East
Aurora. At Gowanda and Zoar the drill passed through the Salina shales,
finding brine, but no salt, in the rock-salt horizon. The limit, north and west
of which rock-salt has not been found in the county, and is not likely to be
found, is a line drawn from East Aurora to Patchen, curving westward near
Boston Corners and thence southward, crossing Cattaraugus creek about

three miles west of Springville. It is, therefore, probable that a well sunk to

392 Report oF THE STaTE GEOLOGIST.

the Niagara limestone at Wales, South Wales, Elmwood, or at any point
within five miles southeast of these places, would pass through a good bed of
rock salt.

Water-Power.

Although there are several large streams in the county, they are not well
adapted to furnish much water-power. In their lower courses, where the
volume of water is large, they either flow across a plain having very little fall,
or, as in the case of Eighteen-Mile creek, lie at the bottom of deep gorges,
where they are practically inaccessible. In the hill region, where there is
plenty of fall, the volume of water is small. Ellicott and Murder creeks

furnish good, but not continuous water-power where they break over the

limestone terrace, and the two branches of Cazenovia creek are capable of
furnishing much more power than is now used. At present it is principally
utilized for local grinding, sawing, ete. At Falkirk some of the power is used
in one or two of the cement and flour mills and, at Holland, in a large tannery.
Beyond these interests, water-power contributes very little toward the manu-
facture of products designed for outside use.

While in most instances I have given the source of information furnished
for this report, I wish especially to acknowledge my obligation to the officers
of the South Buffalo Natural Gas Co. and to Mr. Michael McIntyre, for the
use of maps and records of wells in the South Buffalo and Zoar fields, and to
Mr. J. W. Stearns and Mr. Mook, who have furnished me records of wells
drilled under their supervision. Also to Professor Franklin Barrows, who
has turned over to me original material regarding natural gas, which he

collected several years ago, and which has not heretofore been published.

Note to Page 326.

While the work of deepening the Erie canal was in progress in_ the
spring of 1897, the canal-bottom was exposed all the way from Ferry street
to the harbor. From Ferry street to the railroad bridge, well-defined glacial
markings were found wherever the bottom was covered by clay or boulders.
This portion seems to have been a part of the river bottom when the canal
was made. From the railroad bridge to the harbor the canal-bottom was
glaciated almost continuously. Excellent areas of grooving and_ polishing
were noticed just above the Porter avenue bridge, and again near the New

York Central railroad bridge across the canal near the Terrace.

FIGURE 1

ILewisTon

Salina

GRAND ISLAND

FADS,
Z Ga
Y ‘ ' | } Corniferous
NAWA Si 7a
: ee Bh Newstead |
Nae ee ee See
\ = Mill Grove = ‘
Crittend S+Stofford L
Te Wage HEtion |
2 5 Morcellus
are y Ee ey a
Alden Center, S~ Sot | 3
e | let 5
Town Line tate A OAlden
Wet 3 “or| Encrinal [5
i Grand Trunk pane ana cat iS
Crystal teach Nia Jer oe Ee | }Genesee x
% we UJ
\ Geo a
\ ,M2 ES EAS
ECONOMIC ann GEOLOGIC MAP \
OF « | |
TN yee
ERIE CO..N.Y. \ +: ee
anvotg State | iF 1 E |
Sprin A ; | Wales Centge
IRVING P.BisHop, ® EF : lest atl im | ey
(SSS SS t J P| oe H BURG \ waAL EVs
f | tau TeAw LU ER) 10) SA\NAD s wet
| ; |
a \ a
= Jewel \
Ne h Wales \ |
\\a |
ina =! ee === =|
Le " || | ror MEMUNG
Sites |
8
Basten,
be ities |
Fetes
a

eee G R
ciacore! AS TERRITORY |

ee GAS WELL
ee - QUARRIES mi! LIME
2 CEMENT y
BRICK ano TILE FACTORIES

“et
ey

fe

7

eo
oe
ae:
Oy
a

a

FIGURE 2 rs = _

=| > i, an | (Rosedale. it |
= : '
l — : = :
te a
¢ 2
q De ‘ys Kenmore. E
NJ Neer \ Ds
| hy = qY ~ Ye, CoA gy A.
SS ~ —BOUNDARY \ %, \ =
a cee LINE ~~. Sy Fee) Sa Pee
NY We — | H |
he A = a
Pa ‘ Ss WUE
\! ai BELF LINE
=a AWN E aa
NS —_ p ae
te SES
; , baz ies

Met i a
(ORM Ch PAST
(Ee Ae |

DS0CUG IAC P= a\h fee | id
paau WN lees ret Na)
1 le RA of

U OSES
eee

ad Uest!

See a 2
eel ee) eee
SSS

leo
SHE res =

iS we 5h eteretiitenn ote
: Se ee al E
00 |

ie

viii ) - U fs
Os Ga Le UOOGSO0_J

Hh lj
Ve ee to % ee
| Ne] ESS:
| “ - # HORSESHOE REEF L./4 on essa
| Bs

BUFFALO EAM ATLL,
LH.

Stony Point

MAP SHOWING LOCATION OF BORINGS FOR NATURAL GAS IN THE CITY OF BUFFALO.
The Alinshouse and Buffalo Cement Company's wells are the only ones now productive.

“i
y
‘
ee
r
‘
a

“2 ato

Sis ele

FIGURE 3

GROUP OF GAS WELLS NEAR THE MAIN STREET CROSSING OF THE NEW YORK CENTRAL BELT LINE, BUFFALO,
Productive wells are represented by stars; unproductive wells by double stars.

“sTfP CATJONpoOId-uON = Iv4s eTqnog ‘se3 Suronpoad Mou eave 10 Peupoid oavq Gory sTToA\ —= Iv4g

‘OTVAdNE “ANIT LIAM CNV LAAULY NIV ‘ENVdNOO LNAWAO OTVAang HHL dO SHYOM FHL YVAN STTAM SVD ZO NOILVYOOT YNIMOHS dVK

‘ &
on We
\4
XX
=

6°00)
AadTAyM 3

7

esnanoy
veg

uosky

¥ AANA

pet pene eprop pide fioquaby ox "fie Boas" broqnerne Roe “pon pile eoat = You-brogecg2e asepye .

NVL eHOsTME POGTLION OW GVY4 AEP? KEVE LHE JAOHK# OL LHE BRELVIO GENEXL GONLYAL’ WYIA ALBEEL V“D BEDE

a Fas

> BORLILO" |

FIGURE 5

MAP SHOWING THE LOCATION OF GAS WELLS NEAR JEFFERSON STREET, BUFFALO,
Wells at one time productive are represented by stars; unproductive wells by dotted crosses

siova a2 3A | |e

OL RAUE NUMA AOPABZVIAL HACK ALIGW 242 YO VOITADO THT DYTWORE TAM

ry

baeeano badioh YC allow oriteuborqay (wate Yo balaaunge: ow pyideabory pgit ene de allo

ot
es anv.
zt i . s

S¥9 ONIINGOUd STTEM = xX
ONITIIYG 40 SS390Ud NISTIZM = O +

nl
Ss
ST1UM ONIDNGOYd-NON = 2
Q7al4 SV9 O1v44Na HLNOS™——+
3HL 40 dvW | | \

cs
as
S 1
+

99t

Ac
i

Io
L

9 GaN

_——_s GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.
re et ee La rates (GEOLOGICAL MAP.)

GEOLOGY OF ORANGE COUNTY.

L HEINRICH RIKS, Ph. D.
chai State Geologist. Assistant.

1895.

‘
t
preps a ries i“
Ten Pon Se |
Veep ets
*

LEGEND

GEoLocic Map

, OF

On ance County \.)

HENRICH RIES,

1895

al CHEMUNG

ie | HAMILTON INCLUDING MARCELLUS
eal Ononnaca

real} ORISKANY & ESoPUS

= HELDERBERG LIMESTONES
= MEDINA INCLUDING ONEIDA
yo Hudson River

| TRENTON

ar POST CANBRIAN GRANITE
— WHITE \ Ca BRIAN LIMESTONE

Blue |

a PRE CANBRIAN GNEISS

ba

/
Colde jaan
Montgomery ofBerea 6 devia;

OK\Coldenham

N ew Win iy 4
gilsGaley

rwall\ Canterybury )

scaeeeh
ae
ae

WYNKOOP. HALLENBECK.CRAWFORD CO. NEW YORK & ALBANY.

Report on the Geology of Orange County.

By Herricu Ries, Pu. D.

Contents. Physical Geography, p. 395; Literature, p. 397. Stratigraphic Geology; Pre-
Cambrian, p. 399; Cambrian, p. 400; Trenton, p, 400; Hudson River, p. 401; Melina, p. 401; Helder-
berg, p. 401; Oriskany, p. 402; Esopus, p. 402; Onondaga, p. 405; Hamilton, p. 403; Chemung, p. 404,
Pleistocene, p. 405. Areal Geology: The Warwick Cambrian Limestones and the Granites, p. 405;
The Region along Bellvale Mouutain, p. 410; Area along Skunnemunk Mountain, p. 415; Relations
along the northwest of Skunnemunk Mountain, p. 418; The Region to the east and southeast of
Skunnemunk Mountain, p. 424; Area west of Cornwall, p. 426; Geology of Deer Park Township,
p. 428; Hudson River Shales and Sandstones, p. 489; The Neelytown Limestones, p. 442; Geology of
Newburgh and New Windsor Townships, p. 443; The Highland Area, p. 446; Dike Rocks, p. 457;
Pleistocene Deposits, p. 462.

The following report is principally based on the results of three months’
work in the field during the summer of 1895, and to it is added such
additional information on the geology as has been published by others.

Orange county is situated in southeastern New York, and extends from
the Hudson river on the east to a short distance beyond the Shawangunk
mountain on the west. The county has an area of 838 square miles, with an
east and west width of forty-five miles, and a north and south length of thirty-
five miles. On the east it is bounded by the Hudson river, on the north by
Ulster and Sullivan counties, on the west by Sullivan and Delaware counties,
and on the south by Pennsylvania and New Jersey. The county is well
known on account of its scenery, mineral localities and dairy products.

Topography. In the eastern portion of Orange county, and bordering on
the Hudson river, are the Highlands, a range of parallel hills, nearly all of
them over 1,000 feet in altitude, and separated by shallow valleys. The more
prominent elevations of this region are: Crow’s Nest, 1,418; Butler hill,
1,524; Bear mountain, 1,350 feet A. T.

The Highlands cover about 140 square miles.

West of the Highlands, and separated from them by a fault valley, is the
Bellvale-Skunnemunk ridge, extending in a northeasterly direction from the
state line, on the northwest side of Greenwood lake, to Cornwall. At
Monroe, the ridge is interrupted by a broad, transverse valley, and northeast
of Monroe it has a double crest with steep cliffs.

The fertile rolling country to the northwest has a topography of little

variety, except to the south, the land gradually rising until it merges into the
395

396 Report oF THE STATE GEOLOGIST.

eastern slope of the Shawangunk mountain. This mountain enters the county
from the north, and crosses it in a northeast to southwest direction, passing
into the Blue mountain, in New Jersey. It does not present the steep slopes
and precipitous cliffs in Orange county that it does in Ulster, but is a rounded
ridge whose cultivated eastern slope changes abruptly at the summit to a
wooded one of deep descent on the western side overlooking the Neversink
valley and the intermediate Helderberg ridge. The crest of Shawangunk
mountain varies, within Orange county, from 1,200 to 1,400 feet A. T., being
highest at the northern end.

To the west of the Shawangunk mountain, the Hamilton and Chemung
formations give rise to an elevated plateau, with few longitudinal valleys, but
several transverse ones,

The valleys of Orange county are largely dependent on the geologic
structure, and follow the axis of the folds or the lines of faulting, and are in
general, therefore, parallel to the strike of the rocks. These valleys also form
important lines of drainage.

The Wallkill, which is the largest river of the county, enters it from the
south, and, flowing northward through a broad, shallow valley whose width
increases to the north, passes into Ulster county, finally emptying its waters
into the Hudson at Rondout. Except in the southern portion of the county,
all but one of its tributaries come from the west and northwest. In Warwick
township, the river 1s bordered for twelve miles by a swampy tract, the
Drowned Lands.

The Neversink river, which crosses the eastern side of Deer Park town-
ship, follows the western base of the Helderberg ridge, and empties into the
Delaware river at Carpenter’s Point. It draims the western slope of Shawan-
gunk mountain and the greater portion of the township to the west of it.
The eastern side of the Shawangunk ridge is drained by the Shawangunk
kill, whose water-shed borders that of the Wallkall.

The Ramapo river has its origin in Round pond, south of Monroe, and,
flowing southeastward through the fault-valley in the Highlands, receives
most of the drainage of Monroe and 'Tuxedo townships. In the northeastern
part of the county, the Moodna river and Quassaic creek are important
streams.

Orange county abounds in lakes, especially in the Highland area, and a
few of them are utilized for water supply. Of these, Little pond, near New.
burgh; Little Long pond, near West Point; Mt. Basha lake and Long pond,
south of Monroe, and Greenwood lake, are of importance. The last-named

Rirrs—GerEoLocy oF ORANGE County. 397

lake is the largest in the county, being six miles long and three-quarters of

a mile wide, but only half of it hes within the state.

Many of the lakes are disappearing, on account of swamp-growth
extending from their inlets, or the cutting down of their outlets, and the beds
of former ponds are an important agricultural feature of the county.

The geologic formations occurrmg in the county range in age from the
Pre-Cambrian to the upper Devonian. Nearly two-thirds of the county is
underlaid by the Hudson river slates, as will be seen from the accompanying
geologic map, and the crystalline rocks of the southeastern portion also cover
a considerable area. The other formations occur in irregularly shaped areas
of variable size, but there is a tendency in them all to extend in a northeast
and southwest direction.

Folding and faulting have produced numerous and local complications,
especially along the line of Bellvale and Skunnemunk mountains.

The following bibliography indicates what has already been published
on the geology of Orange county :

Barrett, S. T., 1876: Notes on Lower Helderberg rocks of Port Jervis, N. Y.,
and descriptions of a new Pteropod. Ann. N.Y. Lyc. Nat. Hist, Vol.
XI_, p. 290.

Barrett, 8. T.. 1877: The Lower Helderberg rocks of Port Jervis, N. Y.
Abe ws.9(0), SLIT, p. 385.

Barrett, S. T., 1878: The Coralline or Niagara Limestone of the Appalachian
Syeremie ee J: S. (3), XV... p. 370.

Barrett, S. T., 1878: Descriptions of new species of Fossils from the Upper
Silurian rocks at Port Jervis, N. Y., with notes on the occurrence of the
Coralline Limestone at that locality. dan. NV. Y. Acad. Sci, 1, p. 121,

Darton, N. H., 1884: Preliminary Notes on Fossils in the Hudson River
Slates of the southern part of Orange county, N. Y. A.J. S (38), ”
XXX., p. 452.

Darton, N. H., 1886: On an area of upper Silurian rocks near Cornwall,
eastern central Orange county, N. Y. A.J. S. (3), XXXL, p. 209.

Darton, N. H., 1885: Gives review of geologic relations from Green pond to
Skunnemunk mountains. Sez. Amer. Sup., X1X., p. 7,877.

Darton, N. H., 1885: The geologic relations from Green pond, N. J., to
Skunnemunk mountain, N. Y. Lu//. Geol. Soc. Amer., V., p. 367.

Dwight, W. B., 1880: Calciferous as well as Trenton Fossils in the Wap-
pinger Limestone at Rochdale, and a Trenton locality at Newburgh,

Ni ¥ees.(8), XIX, p.-50.

398 Report or THE STATE GEOLOGIST.

Dwight, W. B., 1880: Description of a new discinoid Brachiopod from the
Trenton at Newburgh, N. Y. A. J. S. (8), XIX., p. 451.

Dwight, W. B.: An interesting geological locality at Cornwall, Orange
county, N.Y. Zrans. Vassar Bros. Inst., I., p. 74.

Dwight, W. B.: The peculiar structure of Clark’s clay beds near Newburgh.
Trans. Vassar Bros. Inst., U1., p. 86.

Dwight, W. B., 1884: Recent investigations and palaeontological discoveries
in the Wappinger Limestones of Dutchess and neighboring counties,
New York state. Proc. A. A. A. S, XXI., p. 384; Nat. Lets. Hour
and Mus. Bull. No. 18, May, 1884, p. 4.

Hunt, T. 8., 1886: Reference to discovery of fossil plants in the Skunnemunk
mountain belt. Min. Phys. and Physiog., p. 591.

Kemp, J. F., 1888: A Diorite Dike at the Forest-of-Dean, Orange county.
A cd S38) KX IVE pe.

Kemp, J. F., 1888: The Drkes of the Hudson River Highlands. Amer. Nat.,
XX Ce:

Kemp, J. F., and Hollick, A., 1893: The Granite at Mounts Adam and Eve
and its contact phenomena. Ann. N. Y., Acad. Sci. VIL. p. 638. ®

Martin, D. 8., 1871: The Coal of. Orange County, N. Y. Proc. Lye. Nat.
Hist. lp. 209:
Mather, W. W., 1842: Report on Geol., Ist Dist. N. Y. Various references.
Merrill, F. J. H., 1886: Ref. On the age of the Green Pond, Bearfort and
Skunnemunk mountain rocks. VV. J. Geol. Surv., 1886, p. 118.
Prosser, C. 8., 1892: Notes on the Geology of Skunnemunk Mt., Orange Co.,
N. Y. Zrans., N. Y., Acad. Sei., X1., June, 1892,

Prosser, C. 8., 1894: The Devonian System of Eastern Pennsylvania and
New York. Bull. U. S. Geol. Surv., 120.

Ries, H., 1891: The Clays of the Hudson River Valley. Trans. N: Y. Acad.
Sci., Nov., 1891.

Ries, H., 1895: The Clay Industries of New York. Ball. N. Y. State
Museum, Vol. IIL, No. 12.

Smock, J. C., 1889: The Iron Ores of New York. Bull. N. Y. State Museum,
Vol. Ti Nori

Smock, J. C., 1889: The Building Stones of New York. Budi. N. Y. State
Museum, Vol. II., No. 10.

Smock, J. C., 1884: Ref., Ann. Rept. N. J. State Geologist, pp. 29, 46 and 51.

Van Hise, C. R., 1892: Ref., Orange Co., p. 415. Bull. U.S. G. S,, No. 86.

Rires—Gronocy oF ORANGE County. 399

White, I. C., 1882: Various references to Orange Co. in Rep. G6, Penn.
Geol. Surv.

Whitfield, R. P., 1879: Discovery of specimens of Maclurea magna of the
Chazy, near Newburgh, N.Y. A.J. S. (3), XVIII, p. 227.

Williams, G. H.: On some remarkable crystals of pyroxene from Orange
Co. “Ne

Ward, L. F., Notes occurrence of plants at Woodbury Falls. st Ann. Rep.,
UO \SPGaiszepcoo 2:

Of the above list of papers the more important are those of Prof. Kemp
and Mr. Hollick, Prof. Prosser and Mr. Darton.

The following is a list of the formations occurring in Orange county,

together with their character and approximate thickness :

Pre-Cambrian, Gueisses, granites and limestones, ——-
Olenellus, ? Limestones, usually impure, 90’ +
Cambrian, Limestones, 200 +
Trenton, Limestones, —
Hudson river, Shales, slates and sandstones, 2,000 +?
Medina (incl. Oneida), Sandstones and conglomerates, 150’—750'
Lower Helderberg, — Limestones and shaly limestones, 25-500’
Oriskany, Impure limestones, sandstones,

quartzite and conglomerate, 50’-150'
Esopus, Slates and sandstones, (50'S
Onondaga, Cherty limestones, 250’
Marcellus, Arenaceous shales and shaly sandstones, 800’
Hamilton, Shales, sandstones, flagstones and

conglomerates, 1,200—1,800'
Chemung, Arenaceous shales and sandstones, 2,250!

_ Pleistocene, Clays, sand, gravel and boulders,

Pre-Camprian. This formation consists of a great mass of gneisses,
gneissic rocks, and some limestones. At times the gneissic rocks are massive
and resemble a true granite. At other localities they present a schistose
facies. ‘These rocks form the Highland region, the northwestern side of
Bellvale mountain, and a series of rounded knob-like Ills extending from
Sugar Loaf village to Newburgh.

The gneiss is usually a mixture of quartz, biotite and feldspar, the latter
often plagioclase. Hornblende sometimes predominates, as in the gneiss of

Bellvale mountain and Tuxedo township. Pyroxene gneisses also occur. The

400 Report oF THE STatE GEOLOGIST.

gneiss forming Sugar Loaf mountain, and the areas to the northeast, is a
granulite gneiss with little or no mica or hornblende.

Bodies of iron-ore are not uncommon and are not confined to any par-
ticular area or belt, although future detailed study of these rocks may show
that they belong to definite horizons. The ore-bodies are generally of small
size, and lens or pod-shaped, and the ore is, in most instances, lean. The two
important ore-bodies are those of Forest-of-Dean and Sterling.

Limestones occur interbedded with the gneiss, but are rare. One bed is
found at Popolopen pond, and another at Fort Montgomery.

The crystalline rocks of this region often appear folded and sometimes
faulted; the thin sections do not, however, afford as much evidence of dynamic
metamorphism as one might expect, The folds of these Pre-Cambrian rocks
frequently pitch to the northeast. Dikes are not infrequent!y met with.

In view of the limited extent of our present knowledge. these rocks can
only be classed as Pre-Cambrian. This is also suggested by Van Hise.
(Bulletin United States Geological Survey, No. 86, p. 415.)

Camprrtan. The rocks of this age are light-colored, generally massively
bedded magnesian limestones. No fossils have been found in them, but their
age is based on: (1) the similarity of character of the several areas; (2) on
their relations to the overlying formations, and (38) on the occurrence of
Cambrian fossils in the limestone of northern New Jersey*, of which they
are undoubtedly a continuation. Their greatest development is in the western
part of Warwick township, and in Lookout mountain, south of Goshen. The
limestones are normally light blue and finely crystalline, but sometimes
become coarsely granular, shaly or even brecciated, as east of Goose pond
mountain and south of Neelytown. Around Edenville they have been
changed by granite intrusions to a coarsely crystalline white limestone.

In Bellvale and Skunnemunk mountains, the limestones underlie uncon-
formably the younger formations, while north of Greenwood lake and east of
Pine hill they are faulted against the gneisses, and the same relations hold
true at Snake hill southwest of Newburgh. In the northeastern part of the
county they are faulted against the Hudson river slates.

The thickness of the Cambrian limestones in Orange county can not be
determined with accuracy, but it is probably not less than 500 feet. In
Lookout mountain, south of Goshen, they have a thickness of about 200 feet.

Trenton Livestonr. There is a small, highly fossiliferous area of this

rock on the River road, about two and three-quarters miles north of Newburgh

* A. F, Foerste.— American Journal of Science, December 1893, p. 435.

‘Ll GNNOYY SLNSWSves
YVINONY 3O SIY¥SS0 SHL ONIMOHS ‘NIVLNNOW SIWAIISG 3C GNS NYSHLYON SHL SO LSAM JZLIZLYVNO ANVYHSINO JO dOYOLNO

| sLV1d

Rres—GEKoLoGY oF ORANGE CouNTY. 401

ferry. In the single exposure known, this rock is a dark blue-grey, shaly
limestone, containing abundant crinoid stems and several Trenton species.
The rock strikes N. 385° E. and dips 40° E.

Hupson Rrver Suares. Two-thirds of Orange county is underlaid by
the members of this formation, which cover nearly the entire area of the
townships of Mt. Hope, Crawford, Montgomery, Goshen, Wallkill, Wawa-
yanda, Chester, Newburgh and Cornwall.

In the western portion of the county, the formation is represented by
interbedded shales, and red, brown or grey sandstones, while in the central
part the slates and shales only appear. The sandstone beds again come in
towards the northeast. Conglomerates are occasionally seen in the north-
eastern part of the county. The slates are black, grey or brown, and often
very fissile. The sandstone layers are often several feet in thickness.

Fossils are rare, but have been found at several localities, notably Sugar
Loaf, Rock Tavern, Greycourt and Goshen. They show a mixed Hudson
river-Trenton fauna.

The country underlaid by the Hudson river formation is a fertile one,
and the outcrops are comparatively few, forming rounded hills and ridges.
These rocks rest unconformably on the Cambrian limestones and gneisses, and
underlie the younger rocks in the same manner. Their thickness in this
county is probably not less than 2,000 feet.

Meprina Sanpstonr. The members of this formation are fine-grained
quartzites, conglomerates, shales and sandstones. The formation has its
greatest development in Deer Park township, where it forms the western
half of Shawangunk mountain. There it consists of a quartzose conglomerate
40-50 feet thick, which passes upward into 700 feet of Shawangunk grit.
This latter is a hard, evenly bedded quartzite, dipping to the west under the
red Medina sandstone, which grades upward into greenish grey shales of the
same age. Another area of Medina age forms Pine hill, east of Skunnemunk
mountain. Here are 60-70 feet of Oneida conglomerate, dipping to the west
over the Cambrian limestones, and passing upward into tlie Longwood red
shales and shaly sandstones, of which there are about seventy feet in
Pine hill.

Their upper members are greenish shales and quartzites, which crop out
south of Cornwall station. They underlie unconformably the Helderberg
limestones.

Hetpersere Lirvestones. There is considerable variation in the distri-

bution and thickness of the members of this formation in Orange county.

26

402 REPORT OF THE STATE GEOLOGIST.

Small patches occur west of Stone Bridge, northeast of Bellvale, northwest of
Monroe and northeast of Highland Mills. The two important areas are the
one west of Cornwall station, and the belt along the western side of Shawan-
gunk mountain, In the latter belt are recognized the Tentaculite, Lower
Pentamerus, Shaly and Upper Pentamerus members. In the Cornwall area,
the Shaly, Pentamerus and Tentaculite are met with. The Scutella limestone
is not found in the county. As the characters of these beds are so
different at the various localities. they are best described in the paragraphs
treating of these regions.

Oriskany Sanpstonge. The two belts of Oriskany which occur within
the county present widely different characters. The western belt forms the
western part of the Helderberg ridge, which extends up the Neversink valley
from Port Jervis. It consists of fime-grained shaly sandstones and impure
limestones, the latter often containing many fossils. The limestones weather
to a soft red rock, from which the fossils may often be dug with a knife. The
beds dip to the westward under the Esopus slates and Pleistocene deposits of
the Neversink valley, but the bedding is almost everywhere obscured, and
there is present a pronounced cleavage, which causes the rock to split into
very thin layers. The cleavage generally dips steeply to the east. There are
also often present cherty bands containing fossils. The Oriskany forms
narrow ridges, and the thickness of the formation is about 125 feet.

The second Oriskany area is along the western side of Bellvale and
Skunnemunk mountains, where it affords a fine-grained red or gray quartzite,
which changes locally to a conglomerate. It is underlaid by the Helderberg
limestone in places, and in turn dips conformably under the Monroe shales.
About one hundred feet are exposed. The grey limestone is everywhere
traversed by innumerable cracks, which produce an extensive and character-
istic pile of debris around each outcrop. The red quartzite does not
contain these slit-like cavities, which are probably joint cracks. The
conglomerate appears im association with the gneiss knobs northwest of
Skunnemunk.

Esopus Stare. This formation consists of black or bluish grey shaly
sandstones, grits and black slates. It occurs only in the eastern part of Deer
Park township, on the western side of the Helderberg ridge, where it rests
on the Oriskany sandstone. The formation gives rise to small narrow ridges,
which may possibly represent step-faults. The probable thickness is about
700 feet, if there are no faults as above mentioned. All the members have a

strong easterly dipping cleavage, which makes a sharp angle with the usually

“NMOHS 713M SI S9SVAVSID SHI

"SIAUSP LYOd JO ISVSHLYON SSTIIN SIVH-3SNO GNV SNO ‘INO avoutivy NI 31lv1is Sndosy

—

a
a*

>
S- aN

I 3LW1d

a he el

“
Pa |

Ruzs—GEoLoGyY OF ORANGE Counry. 4()3

obscure bedding. No fossils have been found in these rocks in Deer Park
township.

Excellent exposures of the black Esopus slate are to be seen in the
railroad cut of the New York, Lake Erie & Western railroad, about a mile
and one-half northeast of Port Jervis. The formation crosses the Neversink
river above Port Jervis and disappears under the drift of the valley.

OnonpaGa (Cornirerous) Limestone. The beds of this age are repre-
sented by a dark grey limestone in layers one to ten inches thick, and
containing numerous black chert nodules of an irregularly elliptical shape,
whose longer diameter is sometimes a foot. The limestone forms Carpenter's
Point, near Port Jervis, in the southeastern part of Deer Park township, and
also outcrops in a small area farther up the valley, near Port Orange.

Weathering dissolves the lime carbonate, and often leaves the masses
of chert projecting several inches above the surface. The nodules sometimes
contain fossils (I. C. White, Pennsylvania Geological Survey, G. 6). The
Corniferous limestone dips gently to the west. The thickness can not be
determined from the exposures at Carpenter’s Point, but White estimates it
at 250 feet.

Hammron Group. ‘This is an important formation in Orange county.
The lower member, the Marcellus shale, consists of a series of dark colored,
bluish black or brown, arenaceous shales, which crop out along the western
side of the Neversink valley. They are fossiliferous at several localities,
notably at Port Jervis and Rose Point, eight miles northeast of it. They
have a low western dip and a steep easterly dipping cleavage. Their thick-
ness, which is in part buried by the drift of Neversink valley, has been
estimated by White* and also by Prosser at 800 feet, which seems very
probable.

The upper member, or Hamilton proper, overlies the Marcellus, but is
not separated from it by any sharp line of demarkation. It forms a series
of arenaceous shales and shaly sandstones in its lower beds, while the upper
ones are thinly laminated sandstones. The lower members contain abundant
fossils. The total thickness in Deer Park township is about 1,800 feet.

The second area of Hamilton rocks forms the greater portion of Bellvale
and Skunnemunk mountains, and has been divided by Darton+ into three
members, viz.: the Monroe shales, Bellvale flags and Skunnemunk con-

. +
glomerate. f

* Report G 6, Pennsylvania Geological Survey.
t The Devonian of Eastern New York and Pennsylvania. Bulletin United States Geological Survey, No. 120.
t Bulletin Geological Society of America, V., p. 367.

404 Report oF THE STate GEOLOGIST.

Monroe shales. hese are dark grey or black slaty shales and slates,
which are usually fossiliferous. They extend around the base of Skunne-
munk mountain, and along the eastern base of Bellvale mountain.

Their thickness in the former ridge is probably not over 200 feet, but
their greatest development is in Pea hill, near Cornwall.

Bellvale flags. These overlie the Monroe shales, and are represented
by a series of thin-bedded sandstones with occasional shaly partings and con-
cretionary layers. ‘They pass into the underlying Monroe shales, and upward
into the conglomerate. Normally, the Bellvale flags are moderately fine-
grained sandstones of grey color. In their upper layers, near the transition
into the conglomerate, they become massive, quartzose and coarse. The
sandstones are also traversed by numerous thin veins of milky quartz. The
flags extend from the New Jersey state line to the north end of Skunnemunk
mountain, where they terminate somewhat abruptly. The thickness of the
Bellvale flags is about 1,000 feet.

Skunnemunk conglomerate. In its typical development this rock is
composed of an aggregate of quartz and some shale pebbles in a matrix of
reddish quartz and argillaceous material. The pebbles are generally one to
two inches in diameter, but sometimes attain a size of several inches. Local
layers of red slate occur interbedded with the conglomerate in the upper
portions and are well seen in the road over the mountain from Greenwood
lake to Warwick. The conglomerate passes downward through a pebbly
quartzite and red quartzitic sandstone into the Bellvale flags. It can not be
said that these intermediate beds of passage belong to one member more than
the other. The conglomerate caps Bellvale and Skunnemunk mountains and
gives rise to high cliffs and steep ledges. Professor Smock has estimated, and

probably correctly, the thickness of the Skunnemunk conglomerate as 300

feet, but in Bellvale mountain, to the south, it is much thicker, not far from 800 —

feet. Mr. Darton considers that the Skunnemunk conglomerate may possibly
represent the Oneonta formation, as the deposition of the latter in central
New York was characterized by an abrupt change in the nature of the sedi-
mentation, or it may represent the coarse Chemung beds of the southern
Catskills or, thirdly, may be a purely local feature.

CurmunGa Group. This formation is only present in the western portion
of Deer Park township. The beds are mostly unfossiliferous sandstones, with
some interbedded shales. The divisions oceurrmg within the limits of the
county are the Delaware flags, New Milford red shales, Starucca sandstone

and Chemung sandstones, of Prosser.

4
4

‘NIVLNMOW YMNNDNYMVHS SHL GNNOYSMOVe YSHDIH SHL NI ‘ONY 39aIY 943843013

SHL SI ASTIVA SHL SO SGIS YSHLYVS SHL LY

‘WOLLOS ATIBAVED ‘Lv1s SHL SNIMOHS ‘ASTIVA MNISYSASN SSOYOY 1LSVa DNIMOO7

It 3LW1d

“OO GHOIMYYS WOaENa7IVH dOOMNAM

Rizrs—Grorocy oF OrancEr County. 405

Pretstocenr. These deposits are represented by the usual accumulations
of gravel, sand and boulders. In the larger valleys, as those of the Neversink,
Shawangunk, and Wallkill rivers, the gravel and sand accumulations are of
great extent and depth. Those of the Neversink valley are in places known
to be over one hundred feet thick. Large boulders are restricted to New-
burgh, Cornwall and Tuxedo townships, in which they are quite abundant.
The alluvial deposits are represented by terraces along the Hudson river and
other streams and by numerous pleistocene lake beds which cover some

40,000 acres. The pleistocene deposits are mentioned in detail hereafter.

Geology of the Warwick Cambrian Limestones and the Granites.

In the south-central part of Orange county is a belt of blue and white
limestone which begins about two miles southwest of Goshen, in Goshen
township and, extending through the western part of Warwick township
with increasing width, passes on continuously for twenty miles into New
Jersey. To the east of the Drowned Lands, and opposite Black Walnut
Island, the belt is about two and one-half miles wide, and continues this width
to Amity, where it narrows to two miles. A branch of the blue limestone
extends from this point to the northeast, and will be described hereafter.
The limestones also extend under the Drowned Lands, and the blue limestone
is found again on the west side, where it passes under the Hudson river
slate. The white limestone occurs only in the main central belt, and is there
closely associated with the blue. The area occupied by each can best be
apprehended by an examination of the map. In Orange county no fossils
have been found in the limestone, but the contained remains found in New
Jersey prove it to be of Cambrian age. The white limestone surrounds two
areas of granite and gneissic rocks, and borders on a third, Pochuck moun-
tain. It is also penetrated by many granite dikes and masses containing
contact minerals.

Several opinions have been advanced regarding the age of the blue and
the white limestones. Keating and Vanuxem (Jour. Phila. Acad. Sci., 1822,
p- 277); C. U. Shepard (4. J. S.i-XXL, p. 323) 5; Cook (1868, Geol. N. J,
p- 310); and Britton CV. J. Geol. Surv., 1886, p. 77-83), considered that the
white crystalline limestone was of Archean age, deposited on the gneisses and
granites, and metamorphosed. The blue limestone was considered Cambrian.

On the other hand, Nuttall (A. J. S.IV., p. 247), Rogers (WV. J. Geol.
Surv., 1840, p. 47-67), Nason (NV. J. Geol. Surv., 1890, p. 25-50), and Mather

consider that the blue and the white limestones are one and the same forma-

406 Report’ OF THE STATE GEOLOGIST.

tion, originally blue, but changed to white in those portions bordering on the
gneissic and granitic rocks. A third possible view is mentioned by Kemp
and Hollick, viz.: that the white limestone is Archean, but metamorphosed
along granitic intrusions, and thus charged with minerals, while the blue is of
later age. In this main belt no actual contact was found between the blue
and the white limestones, although outcrops were found within 200 feet of
each other on the road running due north from Edenville and northwest in
a general way, along the line of Professor Kemp’s section 3, The two are
considerably mixed together on the northeast slopes of Mount Eve. The
writer, however, found exposures east of the road and one and one-quarter
miles west-southwest of Pine Island station, which showed the passage of the
blue into the white. In the main belt the blue limestone becomes graphitic
and more crystalline towards the white. On the east side of Round hill, the
blue limestone is found quite close to the granite and assumes a_ highly
siliceous character, if not actually becoming a quartzite.

Two great knobs of granite, Mount Adam and Mount Eve, penetrate the
limestone. ‘The rock is a hornblende-granite, gneissic in places, and coarsely
crystalline, especially at the quarries, the anhedra forming the granite being
one-quarter to one-half inch diameter. More or less biotite is present, and
augite is common near the margins. The granite is a basic variety, and
plagioclase equals or exceeds the orthoclase. Quartz is often common, and
contains dusty inclusions. The orthoclase is generally microcline or micro-
perthite. The hornblende is black, and is transparent only in the thinnest
sections. It is then yellowish green parallel to a, black parallel to 4, deep
green parallel toc. Brown biotite is usually rare, but it is quite common on
Round hill. Allanite, a rare mineral, is abundant in the granite, and, together
with peematite veins, has spoiled much of the stone for quarrying. Small
zircons and titanite are not infrequent. The granite becomes quite gneissic
at the north end of Mount Eve, preserving the same mineralogic composition,
but the sections show evidences of dynamic metamorphism in the crushed
crystals of quartz, feldspar, etc. Sometimes the granite assumes a structure
resembling quartz-porphyry. Graphic granite was also found on a knob east
of Mount Eve.

The white limestone is coarsely crystalline, with scattered scales of
graphite and, less often, phlogopite. Chondrodite is also present and
increases near the contact of the limestone with the granite.

Contacts. The granite and the white limestone are found in actual

contact in several places, and only a few feet apart in others. Towards the

‘MSAIN SHL GALONYLSEO HOIHM

131d

JO WYG SHL S| GNNOYSMOVE SHL NJ ‘SGNVY] GSNMOYUC SO GN3 HLYON LV YSAIY TMT JO L31LNO

Al 311d

Rizrs—GeroLocy oF OrancEe Counry. 407

contact, the granite becomes an aggregate of light green monoclinic pyroxene
and scapolite, or a granite-like zone of the two is present. itanite is a
constant associate.

Near the contact, great quantities of silicates appear in the limestone
either in bunches or scattered through it. They are brownish green horn-
blende, dark brown biotite or phlogopite, green pyroxene, titanite, pyrite,

calcite and some scapolite. Chondrodite is sometimes present in great

the
K
=
~

wy
White <e Y
»” 2
imestone ON 5
c

3 White
aA

Aa one : 5S Limestone? v ie
A hata i < eA
Ser Mises S
Seay é vv
Line of section M145 W. ure DY el oy
1 160 yda. D 1 Ore ? TIS a ITS Goat ">

FicukE 1. Section from southwest side of Mount Adam, northwest towards the Drowned Lands.

quantities. A good contact is to be seen on the prolongation of Mount Eve
on the farm of Mr. Onderdonk and on that of Mr. J. Hedges. On the
southwest side of Mount Adam is an excellent section across the granite,
limestone and contact zones. (Fig. 1.)* Next to Mount Adam is a very
swampy strip, following which there is a ledge of limestone with much
_red chondrodite. Beyond this comes the granite with the scapolite zone.
Unusually fine scapolite crystals were found here, with interlaced prismatic
pyroxene individuals. ‘Titanite was present in less quantity. The scapolite
zone 1s followed by coarse white limestone, and this, in turn, dips under the
gravel bordering the Drowned Lands.

About two miles west of Amity is Pochuck mountain, the greater

portion of which les within New Jersey. The eastern part of the

Granite

FIGURE 2. Section across the north end of Pocbuck Mountain.

mountain is composed of a coarse-grained granite, which is quarried for
building purposes. The eastern half of the mountain is a biotite gneiss
(508), which strikes N. 20° E.; dips 80° W. Dikes of the granite penetrate

* This section is copied from Prof. Kemp and Mr. Hollick’s paper, previously mentioned.

405 Report OF THE STATE GEOLOGIST.

the gneiss, pyroxene being developed as a contact mineral between the two.
Small knobs of granite also crop out near the road (505) on the west side
of the Drowned Lands, and about one mile north of Pochuck mountain.
There is also a hill of gneiss just north of the cross-roads on the east side
of the road, and about one and one half miles west by south of Pine Island
station. A short distance northwest of this are several outcrops (504),
showing the transition of the blue limestone into the white. Up the short,
steep slope on the west side of the road, is a blue, fine-grained, hard limestone
(504a), with a low western dip.

The blue lmestone, with contact minerals, also crops out in the road.
Not more than six feet from it is a small mass of white limestone, with
eraphite scales. Next to this is a dark strip of rock, made up of contact
minerals. In the field opposite these outcrops, and about 150 feet distant
(504e) is a mass of blue limestone with cavities and calcite streaks. At
the north end of the same outcrop is white, coarsely crystalline limestone,

eradation between the blue and the

while the space between shows every g
white. A large outcrop of the white occurs on an adjoining knoll to the
north. Another outcrop of the blue and the white is in a corn-field about
one-third of a mile to the southeast (506).

The prolongation of the white limestone belt so far south from Mounts
Adam and Eve, without the appearance at the surface of any large igneous
masses, suggests that the Adam and Eve area and the Pochuck mountain
area are probably connected, and may be portions of the same intrusion.

Relations of the Limestones and Hudson River Slates. Two facts greatly
hinder a correct understanding of the relations of the limestones and the
associated Hudson river slates. The area underlaid by these formations in
Warwick township is a rich farming country, and outcrops are few, and,
rood strikes

ra)

again, the limestones in the main belt are often massive, and
and dips are not easily obtainable. On the western side of the Drowned
Lands, the limestone boundary extends from Unionville, northeast through
Gardinerville and, about two miles east of this place, swings around to the
northeast. Near Liberty Corners the blue limestone (502) strikes N. 70° W.,
and has a dip of 15° W. The layers are four to eight inches thick, with
shaly partings. Northeast of Gardinerville the limestone strikes N. 30° E.;
dip, 830° N. W. It is somewhat cherty and variable in color.

At Gardinerville, the slate is exposed under the dam in the bed of the
stream. The dip is west. Northeast cf Orange farm (89) the limestone is

well exposed in a quarry on the west side of the main road from Goshen to

i ~Bl
Agr

Wi

ack».
InuF

Hamilton

Conglomerate

Hamilton
Shales and
Sandstones

_ Oriskany
Helderberg

Limestone

Hudson River

Slates

=F
Wp,

Granite vy ee
Gambrian,white =
Limestone ===.

Cambrian,blue
Limestone
Pre-Cambrian

Gneisses

xv
Cpls
= ey
. | ~V=v
fo =|- VY
aay \ ean Yyv-Vv
EA (ES Ay oy Ae
rae - vs v Sees
Q “OG —~V-Vv
Vv We SS Qos is
See las : ee
we Vv Yvity aE
“XG — We We SS iat abe Via
<V = Vv Vv —Vv Ui; |. =V
SS v SNe noe v=
. any - ry anne Vv =¥//
Viev <¥ Use is) 6
—({V-a~V = ‘ eee v oY
A lara Ries Sa vee Ri dO v ss
AROS i Mey 433 Re
: V=-v gOn Os Vv a
VT Ice * Vy oe ao
Dykes om Ve eee ty
hee x6 ~ Nr eeaXe
ater VASE VL — vy?
| GY Vo A=, Bad
Mines SS eS “j Wie er
= hea VW
Set Ns Mi
tN VG 7a
Va. md
Ne ee
We = Sve AE
ES win = Vv
eae es ~V 3
Nv y
V
oa

GEOLOGIC MAP OF WAItWICK TOWNSHIP.

The sections shown in Plate X, Figures 1 and 3, are drawn alon:s the straight lines terminated by arrows. Scale 1 in, =1 mi.

Ries—Gronocy oF Oraner Country. 409

Warwick. Here it is a very hard, massive rock with an abundance of cherty
layers and broken by irregular vertical joints. The dip is very low to the
northwest. Half a mile southeast of Mapes Corners is Mount Lookout.
This is made up entirely of Cambrian limestone and affords one of the
best exposures in the county. The upper beds are somewhat coarse and
sandy, while the lower ones are fine-grained and less siliceous. They all
dip shghtly to the northwest. Most of the limestone is very hard and some
of the layers half-way up the hill have siliceous laminae which stand out
prominently on the weathered surfaces. Quartz crystals are not uncommon
in the cavities of the rock. There are evidences of fossils in some of the
coarser layers from the summit of the hill, but no good specimens were found.

Southeast of the lill and opposite a farmhouse on the main road is a
ledge of very cherty, moderately coarse limestone. The thickness of the beds
in Lookout mountain is fully 200 feet. This hill is in the main belt of lime-
stone, whose most eastern limit is west of the upper end of Glenmere luke.

There the slate and the limestone are separated by a narrow ravine, the lime
} uy

Mt. Eve

Mt. Adam Stone Bridge

Gr.
NAVI B.

be! H.R. H
iT WSS Gi SEZ

FIGURE 3. Section from Mount Adam to Stone Bridge.

Gr., Granite; W. L., White limestone; B. L., Blue limestone; H. R., Hudson river slates;
H., Helderberg limestone.

stone forming a ledge on its western side. At this point (97) the two are
about seventy-five feet apart, but a few hundred feet farther south on the
west side of the road, they are within six feet of each other. The limestone
here dips to the east and is overlaid unconformably by the slate, though an
actual contact is lacking.

The Hudson river slates extend southward across Warwick township
in a wedge-shaped area which is about five miles wide at its upper border
and thins out at a point about one and one-half miles northwest of New
Milford. They rarely afford good exposures, but an excellent one is seen on
the road from Warwick to Edenville.

One mile west of Stone Bridge, is a small area of Helderberg limestone
(500) resting unconformably on the blue cherty Cambrian limestone. The

Helderberg is a purplish shale containing remains of Bryozoa, Leperditia,

410 Report OF THE STATE GEOLOGIST.

mollusks and trilobite fragments. The species determinable were a Da/ma-
nites, Leperditia alta, Meristella levis, Nucleospira ventricosa and Colospira
concava.* To the east of the Hudson river slate area is the right branch of
the Cambrian limestone belt which spreads eastward to Bellvale mountain
and northward to Sugar Loaf mountain and underlies the broad, fiat
Warwick valley.

From the strikes and dips obtainable, the indications are that the
Cambrian limestone underlies the slates with a constant, though varying
degree of unconformity and which are themselves brought up by low folds;
the Mounts Adam and Eve area being along the axis of a low anticline. The

section adapted partly from Professor Kemp’s paper, is given in figure 3.

Geology of the Region along Bellvaie Mountain.

Bellvale mountain enters Orange county from New Jersey along the
west side of Greenwood lake, and extends to a point about four miles north
of the latter, with an elevation of 1,200 to 1,300 feet A. T., beyond which it
extends as a discontinuous rounded ridge with greatly diminished elevation,
merging into the southwestern continuation of Skunnemunk mountain,
northwest of Monroe. The latter extends, as a high doubly crested cliff-
topped ridge, nearly to Cornwall.

The general structure of Bellvale mountain is that of a compressed
synclinal of Devonian rocks, a portion of whose western limb has been cut off
by a fault, and the missing member replaced by gneiss.

The geologic age of this belt has been, for many years, a disputed point
among geologists. Horton, in his report on the geology of Orange county,
refers to Bellvale mountain, and states that the southeast side, top, and about
one-third of the slope on the northwest side are composed of greywacke and
greywacke slate, standing nearly vertical. 3

On the geologic map of New York, 1844, the area of Skunnemunk
mountain is put down as Hudson river slate. On the New Jersey geologic
map of 1868, Professor G. H. Cook referred these rocks to the Potsdam.

In 1871, D.S. Martin found the first fossils of this belt in a so-called coal
mine on Skunnemunk mountain. (The Coal of Orange county, N. Y., Proce.
N.Y. Lye. Nat. His. 1, p. 259.) Professor Martin states that the coal mine
of Monroe les upon the western side near the summit of the mountain. The
rock is a dark grey siliceous or argillaceous sandstone, carrying carbonaceous

* J. F. Kemp and A. Hollick._On the Granite at Mounts Adam and Eve, Warwick, Orange county, N. Y., and its Contact
Phenomena. Annals of New York Academy of Sciences, VII, p. 638.

*dIHSNMOL YOIMYev/\\
"Q901NG SNOLS JO 1S3M 'S3NOLSSINIT AIWHS SYS8yS0ISH ONIAIHAAO SHL GNV SNOLSSINIT NVINSNVD NSASMLAS ALINYOSINOON/}

PSO CYOIMVYD HOABNATIVH dOOWNAM

is

IA aLW 1d

Rirs—GEoLoGY oF ORANGE Country. 411

matter. The fossils found, fixed the age of these rocks as Devonian, probably
Hamilton. The plant-remains proved to be Lepidodendron (probably L.
gaspianum), Calamites, Psilophyton and, according to Professor Newberry,
Dadoxylon.

The region was still colored as Potsdam on the geologic map of New
Jersey, of 1874, while the area called Hudson river is put down as Silurian
slates. In a paper by Dr. T. 8. Hunt, the Green pond mountain conglomerate
was mapped as greywacke or Upper Taconic (Zrans. Roy. Soc. Can., L., ser.
IV., page 254). The geologic map of New Jersey, published in the Annual
Report of the New Jersey Geological Survey, made no change for the Green
Pond-Bearfort region.

In the New Jersey Geological Survey Report for 1884, Smock gives a
section from Woodcock hill, northwest of Skunnemunk, southeast and east
across Skunnemunk mountain (p. 46), showing the synclinal structure of the
mountain. The subsequent work of other geologists shows the main details
of this section to be correct. Professor Smock calls attention to the fact that
the relations of this Devonian series of rocks are much easier of interpretation
in this locality than elsewhere. He also gives a detailed map of the region
around Bull hill, northwest of Monroe, and notes the occurrence of plant
remains in the Devonian sandstone quarries.

Dr. Merrill studied this series of rocks in northern New Jersey, and the
results of his work are given in the report of the New Jersey Geological
Survey, 1886, p. 113.

In 1892, Professor Prosser gave a resumé of previous contributions refer-
ring to this region, and discussed in detail the plant-remains of Skunnemunk
mountain. N. H. Darton has contributed a valuable paper on the geology of
this region (Geologic Relations from Green Pond Mountain, N. J., to
Skunnemunk Mountain, N Y.) The results of the writer’s work in Orange
county during the past summer, agree in most respects with those of Mr.
Darton.

In Bellvale mountain the synclinal is formed, in great part, of the
Skunnemunk conglomerate. Excellent exposures of it are seen (184, 186) on
the road from Greenwood lake to Warwick, on the summit of the ridge.
Interbedded with the conglomerate are less pebbly beds and streaks of red
slate. The quartz pebbles are often ground and distorted on slickensides.
The conglomerate passes through a red quartzite into the flaggy sandstones
which are seen lower down on the east side of the mountain. These are
everywhere traversed by veins of milk-white quartz (367).

412 Report oF THE STATE GEOLOGIST.

Toward the base of the mountain they become more heavily bedded, and
are succeeded by shales. The conglomerate extends along the crest of the
mountain for several miles north of Greenwood lake, and forms bold cliffs and
ledges at the top of the steep wooded slopes. It disappears southwest of
Long pond, where the mountain breaks up into rounded hills, and does not
reappear again, except at one point, until Skunnnemunk mountain is reached.
This one point is about three-quarters of a mile northwest of Round pond,
south of Monroe.

The quartz-seamed sandstones come up on the other side of the synclinal,
on the northwest side of Bellvale mountain (866), where they are faulted
against the Pre-cambrian gneisses. The sandstones and conglomerate every-
where present abundant slickensided surfaces.

About 800 feet of conglomerate are represented in the sections across
the mountain at the north end of Greenwood lake.

The Bellvale flags are represented along Greenwood lake by grey flaggy
sandstones, often cut by veins of milky quartz. About two miles north of
the state line, the Monroe shales appear as black slaty shales, resembling
somewhat the Hudson river slates, with which they were for a time
confounded. Hamilton fossils are not uncommon. They are abundant in
the slates along the road, where the latter follows a cliff above the lake, about
one-quarter mile north of the Lakeside hotel.

The fossils are much distorted, but the following were recognizable:

Tropidoleptus carinatus.

Spirifer mucronatus.

Liorhyneh WS, Sp.

Phynchonella, Sp.

The Esopus slate, though very abundant farther down the lake, does
not appear north of the state line.

The synclinal fold of Bellvale mountain is often so compressed that the
dips are eighty or ninety degrees.* The Monroe shales are exposed along
the west side of Long pond, two and one-half miles south of Monroe, and
about 500 feet north of the school-house. They here contained a number of
impressions closely resembling Spzrophyton.

North of Greenwood lake, on a small knoll (426), is an outcrop of
quartzite with sand grains and occasional pebbles. It dips to the westward
under the Bellvale flags. Darton has considered it to be Oriskany, and

while it is very probably this, proof is lacking.

* Some of these apparent dips may be cleavage planes.

"INOLSAWIN SHL AG GIVINSONN AYLNNOD SHL SO YSLOVYVHD SHL SNIMOHS +3AQ LNNOW SO LSVS 'ANOLSSWIT SLIHM SO SdOYOLNO

‘OS GHOAMVYD HOAANATIVH dOOMNAM

HA S1WI1d

4

Rims—GEoLtocy oF ORANGE County. 413

Camprian. The Cambrian limestone underlies the drift-filled valley
northeast of Greenwood lake, as far north as Long pond. There are small
outcrops of it along the base of Bellvale mountain (434), west of Moses
Smith’s house, and also in a ravine to the northeast (423). The gneiss
crops out about 200 feet from it, up the hill-side. The rock is light bluish
grey, cherty and massive, and contains numerous slit-like cavities. Scattered
over the surface at this locality are many angular fragments of Oriskany
quartzite and conglomerate, which appear not to have been transported
any great distance. The limestone probably rests unconformably on the
eneiss of the eastern side of the valley.

To the northwest of Bellvale mountain, the Cambrian limestone, which
spreads out over the Warwick valley, as previously noted, rests uncon-
formably on the gneiss. A good outcrop of this limestone is in the corner
of a field just northwest of Bellvale (107). It shows a thin-bedded character,
and has shaly layers. The strike is N. 50° E., and the dip 30° W. Mr.
Darton* notes a very small outcrop of Helderberg limestone on the northwest
slope of Bellvale mountain, and about one-half mile north of the road across
the mountain. The rock is said to be a dark grey, moderately pure limestone.

Only one shell was found in it, and that resembled Strophonella punctulifera,

_ Conrad.

Pre-Camprian Gyetss. The gneiss, which is faulted up against the
Devonian rocks on the northwest side of Bellvale mountain, enters the
county as a belt four miles wide, and narrows rapidly towards Bellvale,
whence it extends northward, as a narrow strip, to Sugar Loaf. It has a
steep dip. Near the fault lime, the gneiss is massive and hornblendic
(188, 364, 365). The strike east of Bellvale (188) is N. 30 to 35° E.;
dip, 80° S. E., and north of Bellvale (188) the strike is N. 25° E.; dip,
30° 8. E. At times the hornblende predominates to such an extent as to
make the rock black. Toward the west the basic gneiss is succeeded by a
more acid phase, containing much orthoclase and mica.

The gneiss retains the acid character over most of the area south of
Warwick and Bellvale. About two and one-half miles due south of Warwick,
several openings have been made for iron-ore in the hornblendic gneiss.
North of the latitude of Lawton, the gneiss area broadens again to form Sugar
Loaf and Goose pond mountains. The gneiss forming these hills is a
moderately fine-grained mixture of quartz and feldspar with little or no mica

and rarely hornblende. The dip is prevailingly steep to the east. Graphite

* Bulletin Geological Society of America, V., p. 380.

414 Report or THE Stare GEOLOGIST.

is often present, especially along the western border of the area in Sugar Loaf
and Goose pond mountains. ‘This graphitic facies is very constant about one
and one-half miles south-southeast of Chester (167). The gneiss here is a
granular aggregate of quartz and feldspar with numerous graphite scales, and
with a strike of N. 25° E. Mica is rarely present. Farther up the mountain
the graphite is lacking. The Hudson river slate occurs in the same field, but
was not found in contact with the gneiss. A fine-grained hornblendic schist
occupies an intermediate position between the slate and the gneiss (167d).

The stratigraphic relations of the gneiss to the surrounding formations
are highly interesting. The western face of the area is very precipitous at
many points, especially at the southwest end.

One and one-quarter miles east of Lawton, the Cambrian limestone crops
out east of the road (193). The rock is finely crystalline, very hard, and in
layers one to two feet thick. Weathering brings out a sub-bedding. The
strike is N. 10° E., and dip 20° E. or towards the gneiss. About 300 feet
to the east the gneiss rises steeply along a fault line. To the north of this,
the slate overlaps the limestone and is faulted up against the gneiss. This
fault line probably dies out to the north. On the western side of Sugar
Loaf and Goose pond mountains is a flat-bottomed valley which narrows out
to the south.

The Cambrian limestone, of which there are several outcrops in this
depression, rests unconformably on the gneiss and is, in turn, overlaid by the
Hudson river slates, which form a narrow strip along the western side of the
valley. The limestone either thins out to the south or is faulted out. To
the north and east it underlies the lowlands and also extends northeastward
to Oxford, appearing northwest of the station.

There are good exposures of the limestone in the valley of Seely’s brook,
two miles southwest of Oxford. The rock is not so hard as that east of
Lawton, and varies considerably in the coarseness of its grain. A sub-bedding
is common and several of the outcrops show a brecciated structure. The
strike is N. 45° E., and the dip 30° E.

The Hudson river shales appear along the road running southwest
from Oxford along the valley of Seely’s brook (208). They are black or
brownish black shales which, in their upper portion, contain thin quartzose
layers. At one locality along the road (203) fossils are not uncommon. ‘The
most abundant are Orthis testudinaria and crinoid stems, also fragmentary
bryozoans. The slate is considerably’ broken and the quartzose layers which

dip 80° KE, of 8. are traversed by numerous slit-like cracks, which are approxi.

'3ANO1D $99VG JO GN HLNOS SHL LY SAIVHS JONNOW SO dOYDLNO ‘by BYNDIY

PLATE VII A

Y hay VV) V/ i Mis LY, WL
“Hf WT. yt
oe ,

YPnt Wii, Lan
7 aa f i
ANY Y LY

Uy,

pp aile:
La 1 TPR
q}

—

bs Uk = LOE)

Y -/ {(crenstord
7 iL) ~ IN v -p/Y

<q) +}
LLAMA “ati

Vy

i)
0.

a,
ty

f ‘f
PTT // Lh, WISE
MET EE oh ed
BT,

(PLL)

OF
4

7 H
YR 4G a)
He eft ret Valley vv

Cs ay

De
ate

Val ays

oy

(olobecy a Rre-Gambrien Cambrian Hudson River Medina, Helderberg Oriskany Hamilton shales Hamilton

includingOneido Limestone & sandstones Conglomerate
V-v-vu Y Wy py
Beye Yi /
== =: Wh WL

GEOLOGIC MAP OF MONROE, WOODBURY, HIGHLANDS, CORNWALL AND A PART OF BLOOMING GROVE TOWNSHIPS,
The numbers on the map refer to field notes and are in part repeated in the text of the report. The straight lines terminated by arrows show the locatiou of sections on Plate XIV. Scale 1 in. 1 mi.

Pleistocene Dikes Mines or
terrace Qvorries.

m= «=

~ os Sa ie
a hes

me im
i. ae "6

: : |
.
> . |
r | | | |
= |
;
~ / | : |
i
a
‘< v/
iN* :
|
' ‘
} - u :
tz ws ‘“ iY
“Se cee
.- ae i. |
ca ¥

Rizrs—GEoL0GY oF Orancr Counry. 415

mately parallel and form an,angle of 60 to 70° with the dip. Overlying the

9
Ss
Hudson river shales with a shght unconformity, is the Oriskany quartzite
which forms numerous ledges along the western face of this ridge. It isa
hard, fine-grained grey or brown quartzite, traversed by numerous cracks
which break the rock into angular fragments and surround each outcrop with
a characteristic pile of debris.

The rock is sometimes massive, at other times well bedded, giving a
strike of N. 25° E. and dipping 40° 8. HE. At such points it contains slaty
or shaly layers, which, however, seem to be rather the result of shearing
action than sedimentation. On the eastern side of this ridge the quartzite is
hard, fine-grained, massive, and of a light red color, traversed by numerous
milk-white streaks of quartz. There are about 100 feet of the quartzite in
this ridge.

On the western side of the ridge, the relations of the quartzites to the
Hudson river shales are probably, as previously mentioned by Darton, those
of an overthrust, since the Helderberg limestone, which underlies the
quartzite at several localities in this belt, is missing, and the outcrops of
the quartzite and shales are so close together that there is no room for the
limestones.

To the west, the Oriskany passes conformably under the Monroe shales,
the two being separated by only a narrow valley.

The Monroe shales are well exposed along the road from the valley
of Seely’s brook to Monroe, and along the “dug road,” crossing the hill
west of Long pond, which is south of Monroe. They are not infrequently

fossiliferous, and at times resemble in appearance the Hudson river shales.

Geologic Relations of the Area along Skunnemunk Mountain.

From Monroe northeastward, the great synclinal fold of Devonian rocks
extends as a high ridge nearly to Cornwall, where it ends somewhat abruptly.
The southwestern end of the mountain is a gentle syncline, while the north-
east end is similar, except that on the eastern side of the mountain the strata
curve over and downward, forming an overthrown anticline.

The crest of the mountain is formed of the Skunnemunk conglomerate,
the characters of which have been already noted. It begins near the Seven
Springs Mountain house, on the ledges a little to the northeast of it, and
extends along the two crests of the mountain, giving rise to steep cliffs and
rocky slopes. A considerable depression lies between the two crests, and its

northern end is occupied by Barton swamp. The conglomerate is about 300

416 Report oF THE STATE GEOLOGIST

feet thick, as previously noted by Smock, and later corroborated by Darton.
It passes into the underlying Bellvale flags, the intermediate beds being a
grey quartzitic sandstone; the transition beds are, however, of less thickness
than in Bellvale mountain, The lower beds of the conglomerate are to be
seen behind the Seven Springs Mountain house, where they are interbedded
with grey laminated sandstones.

The Bellvale flags extend the entire length of the mountain, cropping out
at numerous points on both slopes. They are thin-bedded, flazey sandstones,
which, in their lower members, have numerous shaly and concretionary layers.

Aside from the outcrops on both sides of the mountain, the sandstones
are exposed along the road leading from the main road west of Skunnemunk,
up to the Seven Springs Mountain house (236). About one-quarter mile west
of the Mountain house are the Davidson quarries at the cross-roads. Several
openings have here been made, and a poor quality of flagging obtained.
Some plant-remains occur in the quarry, northeast of the cross-road, and shaly
layers appear in the southern lower part of the quarry face. The quarry is
about 750 feet A.'T. Professor Prosser records the finding of the following
specimens of plants: Psilophyton princeps, Calamites, and aerial rootlets (2)
of the latter.

A short distance to the northeast of Davidson’s quarry, is Davidson’s
coal-mine. This point is about one and one-half miles north of Monroe.
The greyish flagstones of the quarry contain an abundance of carbonaceous
matter, which led the inhabitants to believe that there was coal present.
Remains of Ps/ophyton are numerous in the quarry. The species thus far
recorded from here are, as already observed: Psilophyton princeps, Lepido-
dendron gaspianum, Calamites transitionis and, according to Newberry,
Dadoxylon ; Dawson, however, thinks the last to be Calamites radiatus.

About one and one-half miles northwest of Monroe, on the southwest
base of the mountain, and 300 feet lower than the Davidson quarries, are
several small quarries on the land of O. H. Cooley. The rock is a thin-
bedded sandstone, with shaly layers, which have been polished to a high
degree by shearing. Concretions occur in the shaly layers and also in the
coarse sandstone ledge to the northeast of Cooley’s largest opening. The
shales contain abundant remains of plants, commonest among which is
Psilophyton. Several of the others were submitted to Prof. Knowlton, but
they were too fragmentary for identification. Prosser notes the finding of
Cllulorylon primavum, as identified by Knowlton. The specimen found

by Prosser represented the end of a stem protruding from the sandstones of

Rirs—Geotocy oF ORANGE Counry. A417

Cooley’s quarry. At the time of the writer’s visit in September, 1895, Mr.
Cooley had uncovered the specimen to a length of twenty-nine feet. The
“fossil tree” has a diameter of fourteen inches at the upper end and eight
inches at the lower end. To this point it dips about thirty degrees along
the bedding; the stem then makes a sharp turn, and can be seen extending
downward several feet more at an angle of about seventy degrees. The dip
of the sandstones is about thirty-five degrees to the east.

Most of the rocks on the steep eastern side of Skunnemunk mountain
are grey sandstones, which, in the second railroad cut north of Woodbury
falls, contain plant remains, chiefly Ps7/ophyton.

The hills to the southeast of Skunnemunk mountain, between it and
Hazard pond, or Cromwell lake as it is more commonly called, are probably
underlaid by the Bellvale flags, but outcrops are very scarce, owing to the
heavy mantle of drift. Several outcrops of sandstone were seen about
three-quarters of a mile due north of Hazard pond, and to the north of
this are some arenaceous shales, in which imperfect specimens of Chonctes
were found.

The Monroe shales underlie Skunnemunk mountain throughout its whole
extent, but are best developed along its western and northwestern base.
They are grey to black, fissile to slaty shales, and are not uncommonly
fossiliferous. They crop out along the road south of Baggs clove (242) and
on the eastern side of Skunnemunk mountain, are to be seen at the base of
the mill dam at Woodbury falls, where the dip is nearly vertical. Their
greatest development is in Péa hill, near Cornwall. There they crop out in
great abundance, especially on the southwest side of the hill, where it rises
steeply from Moodna creek (486),

The shale also appears on the eastern side of Pea hill, near the obser-
vation tower on the summit. On the south slope in the middle of a
field about half-way up the hill, is an inconspicuous outcrop of a very
hard, fine-grained red and grey sandstone (484), containing great quantities of
fossils. The rock is strongly cemented together with iron. The red sand-
stone predominates. The following much distorted fossils were observed :
Spirifer, sp.2 Tentaculites, sp. Meristella, sp.¢ Orthis, sp.? Theca, sp.?
Chonetes, sp.? Pehynchonella, sp. ?

Along Moodna river, near the south end of Pea hill, is a cliff of hard
sandstone traversed by numerous joints (485). Only one fossil was found in
it, viz.: Pentamerella avata. Extending up the centre of the cliff is a strip
of fine-grained, black, nodular rock, which is so hard as to break with

27

415 Report oF THE STATE GEOLOGIST.

difficulty. The nodules have a shell which resembles the sandstones into
which the nodular rock shades. A section of this nodular rock shows it to
be a portion of the sandstone which is firmly cemented with iron.

The structure of Pea hill is probably that of a synclinal fold. The
Monroe shales are underlaid by the Oriskany quartzite which, in Pea hill, is a
coarse pebbly quartzite, massively bedded and very hard. There are good
exposures of it along the road at the northeast side of Pea hill, where these
fossils were found :

Anoplia nucleata,

Stropheodonta, sp.?

Leptena rhomboidalis,

Leptoc lia flabellites.

The Hudson river slates no doubt form the bottom of this synclinal
fold, but outcrops are lacking in the immediate vicinity.

The general structure of Skunnemunk mountain is that of a much more
open synclinal than Bellvale mountain to the southwest. But at the northern
end, the flags and sandstones of the eastern limb turn over and downwards
on to the limestones of the Helderberg and Cambrian, as already shown by
Darton.

The Relations along the Northwest Side of Skunnemunk Mountain.

The Oriskany quartzite, which forms the ridge along the west side of
Seely’s brook, southwest of Oxford, turns to the east, cropping out in the
field below the road, half a mile south of Oxford station (144). At this
locality, it is both coarse-grained and finely granular, The next outcrops are
in a field about one mile due east of Oxford and west of the high-road. There
are three small outcrops, which are hard reddish quartzite with white seams
of quartz. Farther east, on Bull hill, are two small areas of the same for-
mation of a more conglomeratic nature, and which rest on the Hudson river
slates. They strike N. 40° W., and dip 55° N. E. This locality east of Bull
hill is of considerable importance as affording an explanation of the strati-
eraphic relations of the rocks in this region. ‘The quartzite area (439) is
underlaid by a thin-bedded, shaly, dark grey limestone striking N. 60° E.,
dipping 35° S. E. In the limestones are numerous fragmentary remains of
bryozoans, crinoid stems and corals, all of them too poorly preserved for
identification. On examination of the specimens Professor Hall pronounced
them to be lower Tentaculite limestone. Some years ago, N. H. Darton

submitted some specimens from the same locality to Professors Hall and

“ZOUNO|Y SO LSSAMHLYON
‘SNOLSSWIN SY43SYS0ISH GNVY SLIZLYVNO ANVYSIYO N3SSM1Lae ALINYOSNOON() 'G SYynNDd!I4

Reo astoae Na 11VH dOOMNAM

Y ‘
;
Pal
ain
i mgiite

Rrrs—GeEoLtocy of ORANGE Country. 419

Whitfield, who identified them as upper Silurian, and recognized the species
Spiriter cyclopterus, Spirifer macropleurus and Orthis oblata.

An actual contact of the limestone and quartzite 1s not visible, but the
former passes unconformably under the latter. The relations of these two are
probably those of an overthrust or overlap, as explained by Darton.*

The Helderberg limestone overlies the Cambrian limestone unconform-
ably. The latter outcrops along a cross-road (440) just east of Bull hill, and
a few hundred feet to the northeast of the Helderberg exposures. It is in
thin shaly layers, which are seamed by numerous hair-like calcite veins. The
rock is also full of cavities containing powdery limonite. In places the lime-
stone is porous and nearly as light as wood, owing to the leaching out of the
lime. It also, at times, presents a brecciated structure. The strike is
N. 80° E., and the dip 30° 8. The Cambrian limestone appears again at the
eastern base of Bull hill, near the southeast end, in the railroad cut at the
south end of the ridge, on its western slope, and on the northwestern side. It
presents variable dips and strikes, and overlies the gneiss of Bull hill uncon-
formably, at least on the eastern and southern side of the ridge, but on the
western slope the limestone is overlapped by the Hudson river slates, which
rest unconformably on the western slope of the gneiss. The relations of the
rocks of the small area are shown in figure 6.

~ The Oriskany quartzite seen east of Bull hill, probably extends to the
north, but is obscured by the heavy covering of drift to a point about one-
half mile south of Round hill, where there is a small area resting on the
gneiss. It next appears in the eastern slope and summit of a ridge between
Round hill and Woodcock hill, again exhibitmg the conglomerate facies,
with an occasional layer of coarse sandy quartzite. The strike on the crest of
the ridge (242) is N. 60° E., dip 30 to 40° S. The Hudson river slates form
the western half of this ridge, extending to and along the southern base of
Woodcock hill, where the stream has cut a deep gorge through them (245),
A short distance southeast of this point, and along the road crossing the south
end of Woodcock hill (246), the Cambrian limestone appears. It is light
blue, finely crystalline, and contains many calcite veins. It strikes N. 50° W.,
and dips 30° N. E. .

The quartzite is again seen at the edge of a small wood, south of the
same road (247). It is here a coarse conglomerate, with a strike of N. 40° E.,,
and a dip of 50° 8. E. The limestone is seen just west of it, and underlies it
with a shght unconformity, dipping 60° 8. E. The limestone also appears at

* Bulletin Geological Society of America, V , p. 367.

420 Report oF THE STATE GEOLOGIST.

the base of the slope in a wood lot west of the previous exposure and south
of the road. but the dip at this point is low to the west. Northeast of the

y by

ASI
Ay
YM

Gneiss Cambrian Hudson Heldeberq Oriskany Hamilton

imestone River Limestone Quartzite Sandstone
lates

FiauRE 6. Geologic map of the area around Bull Hill.
road, at the upper end of a small field, and at the edge of the woods, the
Hudson river slates crop out at the foot of the slope (260), dipping under

the quartzite and conglomerate, and forming the ridge between it and the

‘j f
i be

‘NIVLNNOW LNONOO] SO 30VS NYSLSSAMHLNOS JO LINWAS YVSN SNOLSSWIN NI AYYVNO

WA JLvId

Rres—Gerotogy oF ORANGE Counry. 491

school house to the southeast. To the west of the shale, in the woods, are
large outcrops of massive cherty limestone. It is not well bedded, but an

anticlinal structure is clearly apparent.

My — aan@ <Q
iN ; Ieee ea = .

~ \
ARCS Ch $A

BS SENS Dri ft

FiGuRE 7, Sections along the line of overthrust at the southern end of Woodcock Hill,

499 Report OF THE STatE GEOLOGIST.

The limestone, slate and quartzite continue northeastward in the valley
east of Woodeock hill, with somewhat the same relations.

An examination of the distribution of the limestone, shale and quartzite
east and southeast of Woodcock hill, shows the presence of an overthrust,
which increases to the south, the quartzite covering the limestone. These
relations have been previously determined by Darton, and as the writer
came to the same conclusions, the sectional drawing from Darton’s paper is
reproduced here (Fig. 7). East of the north end of Woodcock hill, a spur
of the gneiss, together with the limestone and shale, appears east of the road
in Baggs clove. The gneiss is seen just east of the road (340), and the
limestone and slate in the woods (341 and 342). The Monroe shales appear
at the base of Skunnemunk mountain to the east. The Oriskany quartzite
was not seen east of the road at this point, but is exposed in the fields a
short distance south. The gneiss, limestone and quartzite disappear to the
north, either by thinning out or faulting under the Hudson river shales.
The thin strip of Hudson river shale, between the gneiss and limestone east
of Woodcock hill is pinched out of place. There is apparently a fault line
between the limestone and the gneiss.

There is a row of gneissoid hills or knobs northwest of the Skunnemunk
ridge, which extends from Oxford in a northeast direction, parallel to Skunne-
munk mountain, and as far as Cornwall. The relations of these to the rocks
southeast and east of them have been already mentioned.

To the west and northwest they are surrounded by Hudson river slates,
which rest unconformably on their slopes. The names of these gneissic
hills are Bull hill, Ranier hill, Round hill and Woodeock hill. There is an
additional small area near Washingtonville. These hills were no doubt
islands in the seas of Hudson river time.

There is a great similarity in the gneiss forming these knobs, the normal
facies being a granular mixture of quartz and feldspar, with little or no mica.
Nearly all of the outcrops show evidence of dynamic action in the invariable
presence of sheared surfaces. The sections often bear additional evidence
of this fact. k

The gneiss of Bull hill is in two areas, a northern, and a southern one
which extends just across the Erie railroad track. The northern area presents
a very steep northwest face. On the summit near the north end, a large
opening has been made for iron-ore. The strike of the gneiss is N. 30° E.
and the dip 40° 8. E. The magnetite follows the dip, and, according to
the old inhabitants of that vicinity, has been worked to a depth of 150 feet.

Pa |

S! LHDId SHL LV TIIH G3S000M 3H

‘SONVLSIO SHL NI NIVLNNOW ANNWANNNYXS ‘'SSIBND NviId¥8Wvoaed JO
‘GNNOYODMOVE BIGGIN SHL OSV SI S¥ SHOOYN NOLTWVH 3O Suv 1437 SHL NO 11H SHL ONV GNNOYND3SHOs SAL

‘GNOd SNOT SSOY¥OV LSVSHLYON DNIMOOT M3IA TWYSN35

X! dLV1d

Rrrs—GrEoLoGY oF ORANGE County. 492

A drift was run in at the foot of the east slope of the hill for drainage
purposes. Both the hanging and foot-wall of the ore-body are of hornblendic
gneiss, outside of which is the normal gneiss. The ore is very lean, and
has a considerable admixture of quartz. No faults or dykes were observed.
A sectional drawing of the ore-bed is here given.

A section of the hornblendic wall-rock shows it to be a mixture of green
hornblende and some plagioclase. Much of the latter is kaolinized. The
hornblende individuals are much bent and broken.

The sections of the normal gneiss show a mixture of quartz and
plagioclase feldspar, with little or no mica. The cleavage and other cracks
of the feldspar are beautifully coated with limonite. Magnetite occurs
sparingly in grains. Fine microperthitic intergrowths were not uncommon.

At the eastern base of Bull hill, near the south end, the gneiss presents

g a gentle

the appearance of being broken by a step-fault, the rock formin

FIGURE 8. Section of Bull Hill, northwest of Monroe; showing iron mine and drift intersecting the
ore-body,

Nw

G., Pre-Cambrian gneiss; H., Hornblendic wall-rock; H. R., Hudson river slates; ©., Cambrian
limestone.

slope on the west side of the wood-road, and a perpendicular one on the east
side, which slopes gently to the east on its other side.

The Hudson river slates pass between Bull hill and the next gneiss
knob to the northeast.

The road north of Rainier hill passes between two knobs of gneiss.
The latter outcrops on both sides of the road (238). It is massive, and gives
no good dips, but the strike is about northeast and southwest. The slate,
no doubt, formerly extended through this cut, but it has been remoyed by
erosion, and is not met with up to a point about 300 feet east of the brook

west of the mill. To the north and south of the road, the slates extend some

494 Report or THE SvrarE GEOLOGIst.

distance up the flanks of the hills. The road swings around to the north and
intersects another, which turns east along the north side of Round hill.
This road traverses the hill until it rises steeply about three-quarters of a mile
west of the crossroads. At this point (241), the gneiss 1s again met, cropping
out along the roadside. It is very massive, and farther up the hill becomes
very hornblendic, The rock is deeply stained with iron, The strike here
is N. 40° E., and the dip 70° 8. E. An opening for magnetite has been
made at the summit of the hill. The slate appears with a western dip
within twenty feet of the gneiss, and evidently rests on it unconformably.
It shows numerous local crumplings. The gneiss extends along the south
side of the road, as far as the school-house at the cross-roads; while the
slate forms the slope to the north of the road. ‘Toward the school-house
the gneiss becomes more granitic and coarse-grained. Layers of graphitic
schist and pegmatite veins are very numerous at this point. Woodcock hill
to the northeast is quartzose gneiss, with much graphite im the exposures
at the north end of the hill. The strike at the north end is N. 80° E.,
the dip 70° E. ‘The constant eastern dip in this range of gneiss hills is
noticeable. A spur of the gneiss crosses the road to the east, and is seen in
the woods within a few feet of the limestone (840). To the north the gneiss

disappears under the slate.

Geology of the Region East and Southeast of Skunnemunk Mountain.

The Cambrian limestones which are seen in the valley north of Green-
wood lake are covered by drift as far as the valley of the Ramapo,
east of Monroe. The limestone extends from a poimt about two miles
south of Monroe, eastward to Turners, and a short distance beyond that point
in a southeasterly direction. The most western exposure is in the road-bed
a few hundred feet east of the Clove mine, and near a large barn. At this
point it is thick-bedded and intersected by numerous joints. A little farther
to the east at the cross-road (220), the limestone is argillaceous and shaly,
with a barely perceptible dip to the northwest. The outcrops show a similar
shaly character at the other end of this cross-road (445) with a low northeast
dip. In the limestone quarry to the north, the rock is massively bedded and
hard. The limestone here is light bluish grey, in layers six inches to two
feet thick, and fine-grained. It has a low dip of twenty degrees to the north-
west. The rock is much weathered along the numerous yertical joints, and
contains many small cavities lined with crystals of quartz and calcite. About

twenty-five feet are exposed,

‘NIVLNONOW MNAWSNNOYS SO LSAMHLYON SONY GIOSSISND V } 11H GNNOY '6 Sand

”.

GUOIMVES NOdENa TVA GONNA

Rirs—Gronocy oF ORANGE County. 495

As the Highlands east of Turners are approached, the dip continues to
be northwest, but becomes steeper. Southeast of Turners, and just east of
the Erie railroad, the dip is N. W. 45°, while in the quarry north of Arden,
where the limestone is seen in contact with the gneiss along a fault line, the
dip is nearly vertical, but in the upper portions of the quarry the layers turn
over slightly, the dip being to the west. The limestone in the quarry is dark
blue, finely crystalline and in layers of variable thickness. The strike of the
limestone is N. 45° E. The contact between the gneiss and limestone in the
upper part of the quarry is easily seen.

When the furnaces at Greenwood and Southfield were running, the
quarry was important as a source of flux.

The northwestern boundary of the Turners limestone area extends from
one mile east of Monroe to the southern end of Pine hill, in Woodbury town-
ship. The eastern edge skirts the gneiss ridge as a line of knolls, usually
covered with a veneer of gravelly drift. Much of this limestone area has a
heavy drift covering, and includes the large, swampy meadow tract between
Turners and Central Valley.

South of Central Valley (277), the limestone strikes N. 50° E., and dips
70° N. W. Northeast of Central Valley, the limestone area narrows very
much and extends up the shallow valley between Pine hill and the Highland
ridge. In this valley it underhes the Oneida conglomerate. At the north
end of Pine hill it dies out suddenly by thinning or faulting, but reappears
in a short strip from Woodbury falls to Mountainville.

Pine hill is a narrow ridge lying east of Skunnemunk mountain. It has
a steep eastern face and a gentle western slope. The members of the Medina
formation, both with a western dip, give rise to the elevation. The eastern
half and face are composed of the Oneida conglomerate, which is a coarse
quartzite in its upper portions, but exhibits the usual aspect of the formation
in its lower beds. The quartzite grades upward into the Longwood red
shales, which form the western slope of the hill. The transition is well
shown in the northwestern slope of Pine hill.

The Longwood shales in Pine hill are of a bright red color; they vary
from a shale to a shaly sandstone, and are about seventy-five feet thick. At
the north end of the hill the shale strikes N. 60° E., and dips 80° N. W., but
this is somewhat steeper than the usual dip. The conglomerate strikes
N. 60° E. and dips 50° N. W. The cleavage is a prominent feature of the
shale, and dips to the southeast. It is well shown in the road-metal quarries
at the southwest side of the hill.

496 Report OF THE STATE GEOLOGIST.

The shales and conglomerate terminate at both ends of Pine hill by
faulting or thinning out. :

The Longwood shales are overlaid by a thin covering of Helderberg
limestone, with small amounts of limonite along the contact. The outcrops
of the Helderberg are a short distance northeast of Highland mills. They are
siliceous in character, and the following fossils have been recorded by
Darton: Orthis oblata, Leptena rhomboidalis, Spirifer macropleurus. The
Helderberg limestone dips unconformably under the Monroe shales, due
to a probable overthrust; but no actual contacts are observable on account
of the drift. Another exposure of possible Helderberg limestone occurs
one mile south of the Highland mills station (271).

The Area West of Cornwall.

West of Cornwall station is a small ridge holding several members of the
Medina and Helderberg formations. The relations of this area were briefly
referred to by Professor W. B. Dwight* some years ago, and subsequently in
greater detail by Darton.t Figure 10, giving map and sections of this area,
is adapted from Darton’s paper.

The eastern side of the hill, a few rods from the Erie railroad, is formed
of coarse-grained red siliceous conglomerate (Oneida), with red sandstones
and shales of Medina age. The conglomerate is massive and the bedding
irregular.

At the northern end of the hill, in a cut of the New York, Ontario and
Western railroad, there is exposed a section of the Helderberg limestone,
which hes west of and over the Medina beds, forming the eastern face of
the hill.

The members exposed in the cut are:

Medina sandstones, shales and conglomerate, . . . . 25 feet.
Tentaculite limestone: 2-7. 45 (a eee ee
Pentamerus and: shaly limestone, -2- 5 5.9.0 Sn 20

The beds strike northeast with a dip of nearly 90°, and there is no sharp
distinction between them. Veins of quartz and limonite are common along
the bedding planes.

There are several exposures south of the road crossing the ridge and at
points where limonite has been mined, but as they were covered with debris

at the time of the writer’s visit, Darton’s account of them is quoted :

*W. B. Dwight, Trans. Vassar Bros. Inst.
+N. H. Darton, A. J. S 38, XXXI., p 209.

a o4 ati f
va eezmeealltt

Goos:

Fig.4. SEO Pine ou
{NS aaa

Rirs—Grontocy oF Ornanck County. 427

“In a small quarry, about one hundred feet south of the cross-road, the
water-lime rocks are exposed for a thickness of about three feet, and the

sandstone outcrops a few feet to the east. The dip is N. 65° W. 85°, and the

Ficure 10. Map and sections of Region west of Cornwall.

M., Oneida conglomerate; L., Longwood shales; T., Tentaculite limestone; P., Pentamerus limestone ;
§., Shaly limestone; O., Oriskany quartzite; H., Monroe shales.

thickness is twelve feet. The Pentamerus and Water-lime disappear by

thinning out or faulting, and the Shaly limestone lies directly on the Long-

wood shales, while along the contact are beds of limonite. The Shaly

428 Report OF THE STATE GEOLOGIST.

limestone contains an abundance of. fossils, which are easily obtainable in
the limonite pits south of the cross-road.”

The Helderberg rocks probably extend around the Oriskany of Pea hill
to the southwest, but there are no outcrops, owing to the heavy covering of
drift.

The Longwood shales at Cornwall are light-colored, thin-bedded quartz-
ites in their upper members, and red and green shales in their lower ones.
To the east they are underlaid by the Oneida conglomerate. This conglomerate
forms another ridge further west. Northeast of Mountainville, the Longwood
shales crop out along the road to Orr mills.

Geology of Deer Park Township.

Shawangunk mountain extends across the eastern edge of the township,
and separates it from Greenville and Mount Hope townships to the east.
Its rounded crest has an elevation of 1,200 to 1,400 feet, being highest at
the northern end of the township. The lowest point im the ridge is west of
Otisville, where the Erie railroad passes through. The cultivated eastern
face of Shawangunk mountain is underlaid by Hudson river slates and
sandstones, while the steep, wooded western face is formed of sandstones
and conglomerates of Medina age.

The Hudson river formation consists of westwardly dipping shales and
red and grey sandstone beds of variable thickness. No fossils were found
in them at this locality. These beds underlie the Shawangunk grit with a
slight but constant unconformity. The boundary between the two along
the crest of the mountain is generally marked by a swamp, along whose
western side the Oneida conglomerate rises as a low cliff. The sheared
surfaces give evidence of movement along the contact of the slates and
conglomerate. There are, also, along the contact, numerous small fissure-
veins bearing lead and zine intermixed with quartz. The quartz crystals
often show a fine zonal structure, due to their intermittent growth. A
breccia occurs in the vein at Guymard, six miles northeast of Port Jervis.
The fissure vein at this locality is the largest found in the county. It is
three to four feet wide and several hundred feet long, and has been exten-
sively exploited in former years. It is no longer worked. The vein occurs
in Shawangunk grit, but probably extends down into the conglomerate.
The ore consists of galena and sphalerite disseminated through quartz. The

quartz crystals often oceur in radiating clusters. Another opening for lead

Wk eras

tT NG kse,

TCL Mee ana br vy byte tehe in ae ‘i ;

ey

Rai yes iy es
rnb the Ouekone of Pas. ite
ying fb the heavy Boyer ne cna
ee |

7 a a C
SC OPA oe

ie
een

—)

eT Tee WVee OTRAS,’

. + - ielomernte

B Cah

mo). CREST]

"
wae es. rahe]
‘ at ;
nA nUStates }
at <i
i, F
edi shalew and
=) +% a :
(VRPT TTY tovad
le writ wHtiha
ree Line Dae a linig
t;} eiie iy Wy hie ; iL }
¢ oe
i b, "
htt Phe sheared,
aie ea
the woaher anid \ eee
a : 5
if ipninll: fasting
t =
; Abe. viene hs be "
2G; PUREE ETE STRIS }
~ vel ;
anh @ WY OER, i
ak it Biot Sheen é
F “tha EE. it te c a or

4 | Mrew Phe (io,
yronanO © posed ein Qe liv DOSY ad Nie
atixttouP .. anotasmid ezisnD eee is)
m iw “ti mia’ MIHeKwerT ASTAUHO $O 4AM DIDOLOM —

not! rok

,
4

Rirzs—GroLocy oF Orance Counry. 429

and zine has been made at the summit of the ridge above Guymard, also at
the summit west of W. C. Tymeson’s house, three-quarters of a mile north of
Otisville.

The unconformity between the Oneida conglomerate and Hudson river
slates is finely seen in the railroad cut, half a mile west of Otisville, and also
on the north side of the road from Finchville over the mountain to Guymard.
This unconformity indicates an uplift at the close of the Hudson river period,
and erosion of the surface of the Hudson river deposits. Considerable
folding also took place. The Oneida conglomerate and Medina sandstones
were deposited during a period of increasing submergence.

In the lower portion of the Medina formation there are about forty feet
of coarse quartz conglomerate, with interbedded layers of shale. This passes
upward into the Shawangunk grit, which is extensively opened in the
quarry west of Otisville. The rock dips 30° W., and strikes N. 40° E.
It is a fine-grained, bluish grey, gritty quartzite, in layers four to twelve
inches thick, and of very constant character. In the topography it creates
steep wooded slopes covered with a stunted growth of trees. The grit
has a thickness of about 750 feet. It passes upward into sandstones and
shales of Medina age. The sandstones are seen on the western slope of

. the ridge along the road from Finchville to Shin hollow, and a short distance
before reaching the railroad track. They are thin-bedded red sandstones and
shaly sandstones in layers from one inch to a foot thick. At times they are
micaceous and sometimes have small grains of pyrite, as above Guymard.
The strike above Shin hollow is N. 40° E., and the dip, 60° W. (Elevation,
910 feet A. T.) Along the road across the mountain east of Greenville, the
strike is the same, but the dip is 34° W. The red sandstones pass upward
into greenish grey shales, which are exposed in the railroad cut south of
Shin hollow. They are very fissile, and the surface of the thicker and harder
layers is covered with reticulated cracks.

West of Shawangunk mountain is a depression, followed by the Helder-
berg ridge holding the Helderberg limestones and the Oriskany and Esopus
-formations. The Helderberg ridge, with its subordinate crests and ridges,
is parallel to the Shawangunk mountain, from Port Jervis to the northern
limits of the county, and beyond. The structure of the ridge is that of a
monoclinal, with a system of gentle transverse flexures, each hill representing
a low anticlinal, while the roads which cross the range lie in the synclinals.

All the rocks in this ridge have a prominent cleavage, which becomes

more marked with the ascent-in the series, and the bedding is often totally

430 Report oF THE STATE GEOLOGIST.

obliterated. Owing to the heavy covering of forest growth, outcrops are
comparatively scarce. The best sections to be obtained are at the’ southern
end, east of Carpenter’s Point, and at the northern end, east of Cuddeback-
ville, and chiefly on the property of Cornelius C. Cuddeback.

The lower members of the Helderberg limestones are separated from the
upper beds of the Medina, which they overlie with a possible slight uncon-
formity, by a narrow, shallow valley. The Coralline limestone may lie in this
valley, but if it does, the drift covers it entirely and, furthermore, it must be
but a few feet thick in places, as at Shin hollow, where the Medina and
Helderberg are found quite close together.

About three miles southwest of Otisville, on the land of Mr. Cuddeback
previously mentioned, are several small parallel ridges, with steep eastern
slopes, which illustrate fairly well the Helderberg sections at this locality.

The first ridge is a few feet west of the road, and the south end of it is
right behind Mr. Cuddeback’s house. At this point, and near the summit
of its short, steep eastern slope, are small ledges of the Tentaculite limestone
(62a). Itis a hard, fine-grained, dark bluish rock, with a sub-bedding that
shows prominently on the weathered surface. The beds strike N. 30° E.,
and dip 35° N. W. There is an irregular cleavage, which dips steeply to
the southeast, and along which the rock parts very easily, while it breaks with
difficulty parallel to the bedding.

The total thickness of the Tentaculite limestone exposed in this ledge is
about twelve feet. Certain layers contain abundant remains of Leperditiev and
Meristina, and the lower layers of the ledge also furnished a few specimens
of Fuvosites minima.

Ledges near the summit of the same ridge, but about 600 feet farther
north, consist of layers of impure and sometimes shaly limestone (62b),
which contain an abundance of fossils, indicating a mixture of Tentaculite
and Lower Pentamerus faunas. The species found were: Leptena rhomboi-
dalis, Stropheodonta varistriata, Rhynchonella, sp., Actinopteria, sp., Cypricar-
dinia lamellosa, Zaphrentis, sp., Leptostrophia, sp., Pholidops, sp., Spirifer

Vanucemt, Dalmanites, Beyrichia, cluding one large form about three-
quarters of an inch long.

At the south end of the ridge and just west of 62a, 1s a second and
somewhat lower crest, formed of a hard, bluish grey, fine-grained limestone,
with conchoidal fracture and irregular cleavage (62c). It contains no fossils
and dips westward under a coarsely granular limestone, which forms a small

knoll (68), surmounted by a walnut tree. It seems to be a portion of the

‘ONIMSHLVSM OL SNG 3dYHS YVIINDSd SHL ONIMOHS ‘Wvdy LNNOI SO 3dO1S 1SSM NO 4301N08 SNOLS3WNI7

WX 43LW1d

eg
age

oe
Tee
ere

Ries—Grotocy oF ORANGE County. 431

Tentaculite, for the lower layers of the knoll contain Tentaculite fossils.
The limestone beds of the knoll dip 35° N. W., and strike N. 40° E.; their
total thickness is about six feet, and they probably represent the transition
from Tentaculite to Lower Pentamerus. Strophcodonta varistriata is present
in considerable abundance.

These beds are overlaid by eight feet of Pentamerus limestone, which
forms a second knoll, and contains a number of imperfect fossils, besides an
abundance of Pentamerus galeatus, Favosites and Stromatopora ct. concentrica.

These Pentamerus beds dip northwestward at the usual angle,
forming a short ridge about fifty feet to the northwest. The lower beds
of this ridge are the Pentamerus limestone, which passes into the Cats-
kill shaly limestone, forming the upper half of the section exposed in
this ridge.

The Catskill shaly beds strike N. 40° E. and dip 35° N. W.; they have
a pronounced cleavage, and are sometimes quite arenaceous. The usual
number of distorted fossils is present, with Spiérifer macropleurus in great
abundance. ‘The other species from the shaly layers which were identified
with certainty, were: Spirifer cyclopterus, Orthothetes, sp., Leptena rhomboi-
dalis, Spirifer perlamellosus, Fehynchonella, sp., Calospira, sp., Pholidops, sp.

The lower, more massive layers, exposed in the eastern face of the
“ridge, and representing the transition from the Pentamerus to the Shaly
limestone (66a), afforded Orthis oblata, Ehynchonella, sp., Fenestella, sp.,
Stropheodonta punctulifera, Hatonia singularis, Stropheodonta Becki, Celospira
dichotoma, Spirifer cyclopterus, Stropheodonta varistriata, var. arata, Penta-
merus galeatus, Havosites, sp., Astylospongia inornata, Orthis, sp., Dalma-
nites, sp., and Ostracode remains.

The total thickness of the Pentamerus limestone in this ridge and the
two knolls (63) previously mentioned, is about fifty feet.

The Catskill shaly limestone beds exposed in the short ridge aggregate
about fifteen feet in thickness.

There is a depression about 3800 feet in width between ridge 66 and the
next one to the west (67), which is formed by the cherty limestones and
arenaceous shales of the Oriskany. This ridge skirts the Neversink river.
The upper shaly layers apparently do not contain any remains, but the lower
cherty ones are very fossiliferous, and extend nearly to the summit on the
eastern slope of the ridge. Lzptocwlia flabellites and Spirifer arrectus ave
present in great abundance, while the other species found were: P/atyostoma

ventricosum, Platyostoma depressum, Beyrichia alta, Platyceras, sp., Pehyncho-

432 Report oF THE Svratre GEOLOGIST.

nella, sp., Tentaculites, sp. The total thickness of the Oriskany exposed in
this ridge is about one hundred feet.

There are several ledges of Catskill shaly and Lower Pentamerus lime-
stones in Mr, Cuddeback’s lane, south of ridge 66, but their character is the
same as in the outcrops previously described.

The accompanying sketch gives the section from east to west across Mr,

Cuddeback’s land.

Neversink Riv,

O Co < 2
2 Xx 7 Sy
% %, y Be) %,
2, ‘4 Ya a ct “yz
es WD a eS
4, %
A Q
= &

FiGurRE 11. Section across the Helderberg ridge, two miles southwest of Otisville.

The approximate thickness of the different members, as exposed in this
section, 1s:

Oriskany shaly and cherty limestones, . . . . . 75 feet +

Catskillshaly: limestone, a 2) et eee
Lower: Pentamerus‘iimestone; =~) -) “>. 2 "6h e
Tentaculiteslimestone:: oi es 2 eee eee

The next good series of Helderberg exposures is four miles southwest of
Otisville, and one mile slightly northeast from Rose Point. The greyish blue
Helderberg limestone forms a series of low ledges at the southern end of a
large ridge. These ledges are in a field west of the road, opposite a large
pond. About fifty feet of cherty limestone of Lower Pentamerus age, are
here exposed. Fossils are abundant, and nearly all of them are silicified.
These layers are also probably near the transition from the Lower Pentamerus
to the Catskill shaly limestones.

The following species were determined : Spirifer macropleurus (common
in the upper layers), Ovthis planoconvexa, Trematospira formosa, Orthis
biloba (common), Cyrtina Dalmani, Leptena rhomboidalis, Dalmanites
micrurus, Spiriter arrectus, Pentamerus galeatus, Spirifer perlamellosus,

Strophcodonta, sp.. Bryozoans on Loxonema, Lichenalia, sp., Lehynchonella,

b)

sp., Zauphrentis, Havosites, Orthothetes, sp. Lingula, sp., Aulopora, sp.,

1 |

Cladopora, Sp.

“ONNOYDAYOS SHI NI

NMOHS 113M SI SNOLSSWIT SLIKM SHI

WX JLW1d

‘HLNOS SHL WOYS 3AZ LNNOW SO MIA

<7

HoTEouhyED MOSENSAVH dOOMNAM

Rres—GrEoLoGy oF ORANGE CounrTy. 433

The same beds are much better exposed in an old fime quarry in the
woods (76) a few hundred feet to the north.

The Pentamerus limestone is there well exposed with a thickness of
about thirty feet. The beds strike N. 40° E., and dip 45° W. Fossils are
abundant in the upper half of the section, the recognizable ones being:
Pentamerus galeatus, Spirifer perlamellosus, Spirifer cyclopterus, Leptana
rhomboidalis, Anastrophia Verneuili, Astylospongia inornata, Lehynchonella
equivalvis, Atrypa reticularis, Zaphrentis, sp., Havosites, sp.

Stromatopora concentrica is very abundant near the base of the section,
the lower layers of which may represent the upper part of the Tentaculite
limestone.

About half-way between 39 and 76, and a few feet farther to the east,
is a small quarry by an old limekiln (13). The beds exposed here are
much sheared, dark grey Tentaculite limestone, containing abundant remains
of Meristina, Leperditia, Spirifer Vanuxemi and Stropheodonta varistriata.

From this exposure to the Shawangunk grit exposures at the base of the
mountain to the east, is not less than 600 feet; there are, however, no out-
crops. Just what formations underlie this interval is uncertain. The red
Medina sandstones probably underlie a portion of it, and they crop out in
the same valley about two miles farther south. The Coralline limestone may
also be here, but if so, is concealed by the drift.

On the slope of the field bordering the river, and about fifty feet east
of outcrop 39, there are several outcrops of grey and blue-grey, shaly and
arenaceous limestones of Oriskany age. Their total thickness is probably not
over fifty to seventy-five feet. A prominent easterly dipping cleavage exists,
but the dip could not be determined (40). Fossils are not uncommon, and
are abundant in the calcareous layers, especially in the outcrops near the foot
of the slope. The list of species collected is as follows: Avicula, sp., Penss-
dlaeria, sp., Chonostrophia complanata, Leptocelia flabellites, Tentaculites
clongatus, Platyostoma depressum, Strophostylus ?, Discina grandis ?, Spirifer
arrectus, Merista lata, Pterinea, sp., Tentaculites, sp. Stictopora, sp., Edrio-
crinus sacculus, Leptocelia dichotoma, Lingula, sp., Hatonia peculiaris.

The Oriskany forms a series of ledges on the west slope of the hill, on
which the limestone ledges 39 and 76 occur. The most southern outcrop
on the ridge is just west of 39, where there are small ledges (40) of arena-
ceous and shaly limestones, Fossils are not uncommon in the more calcareous
layers, and the following species were found at this point: Sp/rifer arrectus,
Bryozoa, Stictopora, sp.. Edriocrinus sacculus, Leptocelia dichatoma, Platyo-

28

434 Report oF THE Srare GEOLOGIST.

stoma depressum, Lingula, sp., Hatonia peculiaris, Meristella, sp., Discina,
sp., Zentaculites, sp. Thickness here fifty to seventy-five feet.

From this point the Oriskany extends northward along the base and
western slopes of the Helderberg ridges. It consists of shales and impure
shaly limestones, which at times are very arenaceous. ‘The usual strike is
N. 30° E., and there is a pronounced cleavage.

From locality 40, the Oriskany extends southwestward to Port Jervis,
forming the western face of the Helderberg ‘ridge. The formation preserves
the same characters that it exhibits east of Cuddebackville, but there is an
apparent increase in thickness, and east of Carpenter’s Point the Oriskany
must be 100 to 125 feet thick.

The Exopus slate (= Cauda-galli grit) is first seen east of Huguenot, along
the Neversink river. It increases rapidly to the southeastward, being no less

c H.R

FIGURE 12. Section across the Neversink valley at Cuddebackville.

H. R., Hudson river shales; M., Medina; P., Helderberg limestone; O., Oriskany; D., Drift;
H., Hamilton; C., Chemung.

than 700 feet thick east of Port Jervis. The formation consists of black, fine-
grained slates, passing upward into grey grits. The members have a marked
easterly dipping cleavage, and the true bedding is rarely visible. The black
slaty members are finely exposed in the railroad cut of the Erie railroad, one
and one-half miles northeast of Port Jervis, while the grits appear along the
Neversink river, especially southeast of Huguenot.

The Esopus formation gives rise to narrow, rough ridges, which at times
suggest the presence of possible step-faults, but this fact is not certain. To
the north, the Esopus slate passes under the alluvium of Neversink valley,
north of Huguenot.

The Helderberg formations reach their greatest development in the

region just north and south of the boundary line between New York and

‘SIVYENIW LOVINOD HLIM Q39YVHO SNOLSSINIT SLIHM ONILVYLSNSd (YSIWWVH AG GANYVW) SLINVYD JO 3xIG

pase

AIX 311d

N3JAVH dOOMNAM
a

Rizrs—Gronocy oF OrAnGE County. 435

New Jersey, and their thickness is considerable. The following section is

shown in Bennett’s quarry (Barrett, 1878) :

Metitacmire limestone fens et). s+ ss «80. feet.
PavOSie MMeCStON@we eS Sunless. 2 Ato 6 A
Wowemeentamenis hmestone.s ....0). 5... . 50
Delthynethalyelimestone; ys). 4. ss. 2 175
Upper Pentamericrimestone. .. °°. 2. .,. . 250 “
Cis nyeeanestONe we ew) a | eC. 100
Peonucnsl temerity eetee. |... 500 to 800 “

This entire section is not exposed in the face of the quarry, but is
included in the ridges to the west, between the quarry and the railroad. The
fossils are abundant in nearly all the layers, and a full list has been given by
Barrett. The upper portion of the Upper Pentamerus is noteworthy on
account of being crowded with trilobite remains. The relation of these beds
to the Oriskany has been suggested by Barrett and demonstrated by
Beecher.* They form the crest of the ridge known as the Trilobite ridge,
in whose southeastern face the quarry lies.+

Between Bennett’s quarry and that east of Cuddebackville, there are
few outcrops of the Helderberg limestone. There is a good exposure of the
shaly limestone at a point just south of the intersection of the roads from
Shin hollow and Huguenot (77). It strikes N. 40° E., and dips 60° W. (540
feet A.'T.) Fossils are not uncommon, especially Spirifer macropleurus,
Latonia medialis, Leptostrophia Becki, Orthostrophia, Colospira imbricata,
Orthothetes Woolworthana, O. punctulifera, O. radiata.

e No exposures of the Clinton or Niagara were found, though they occur
in Nearpass’s quarry, south of the state line.

The Oriskany sandstones and impure limestones and the Esopus slates
and grits dip westward under the gravelly dip of the Neversink valley, and
the middle and upper Devonian formations rise from the valley on its western
and northwestern edge.

The Onondaga limestone unconformably overlies the Esopus slate at
Carpenter’s Point (83). It forms Carpenter’s Point and crops out along the
road opposite the cemetery entrance. It is a grey limestone, in layers a few
inches thick, and contains numerous elliptical flint nodules, from one inch
to a foot long. The weathering of the limestone give it a rough surface,

caused by the irregular projecting chert nodules. ‘These nodules sometimes

* Amer. Jour. Sci., Vol. 45, p. 410, 1892.
+ Mr. Gilbert van Ingen has given the writer considerable information concerning the region east of Port Jervis.

436 Report oF THE STATE GEOLOGIST.

contain fossils* The Corniferous limestone sometimes has a dip of 20° to the
west. It extends northwestward up the Neversink valley, but is buried by
drift. A small outcrop occurs north of Port Orange, in the rear of C, Norris’s
house, with a strike of N. 50° E. and a dip of 70° W. Some of the layers at
this locality are quite shaly. The thickness of the Corniferous limestone at
Port Jervis is given by White* and Prosser as 200 feet, and this seems ¢
very reasonable estimate.

The Marcellus begins as a ledge of hard grey slate at the bend of the
Delaware river, with a cleavage dipping steeply to the southeast, and extends
up the Neversink valley, the lower members being buried under the drift,
the upper ones dipping under the Hamilton shales. At the north end of
Port Jervis, the Marcellus is exposed at the base of a steep hill, and here
consists of bluish black, fine-grained shales, which dip under the Hamilton
rocks that are exposed farther up the hill. The dark arenaceous Marcellus
shales also outcrop at the base of the ridge along the western side of the
Neversink valley. Those at the base of the hill along the railroad, at Rose
Point are, according to Prosser,} probably near the boundary between the
Marcellus and the Hamilton.

The total thickness of the Marcellus shales in the Neversink valley is
about 800 feet. The Hamilton rocks which overlie them have a thickness
of about 1,400 feet in Deer Park township. They consist of arenaceous
shales and shaly sandstones, passing upward through a calcareous zone
into argillaceous shales containing fossils.

C. S. Prosser has noted a number of Hamilton localities within the
township and a list of the fossils found at each. ‘They are, beginning at the
south, as follows:

Arenaceous shales and sandstones of lower Hamilton age forming ledges
of a high hill just north of Port Jervis (1,477 Al of C.S. P.).

One mile and one-half north of Port Jervis are coarse-grained ledges of
arenaceous shales and sandstones on the east side of the road (1,477 A2 of
O.S. P.). They contain Spirifer granulifer in great abundance.

A short distance farther up the road, are coarse, fossiliferous, arenaceous
shales, forming ledges on the hillside above the road (1,477 A8 of C.S. P.).
This zone, which was called Genesee by I. C. White, contains numerous fossils.

On the east side of the road, a quarter of a mile south of Sparrowbush,

occurs another ledge consisting of coarse arenaceous shales, which carry
* Pennsylvania Geological Survey Report, G. 6.
+ Bulletin United States Geological Survey, No. 120.
¢ Tbhid., p. 45

“A1lWIS YSAIY NOSGNH 3O SI GNNOYSSHOS AHL NI 3dO1S SHL !31WV1S YaAIY NOSONH ONY SNOLSSWIT NVIYSWVD Ad GaldNDDO S$! NSBSM1LEE
ASTIWA SHL ONY ‘SLIZLYVNO ANYYSINO SI 1357 SHL NO TIIH BSH] ‘LHDSIY SHL NO NMOHS ‘NIVLNNOW GNOd-3SOO5 GYYMOL HLNOS DNIMOOT M3A\A

7

‘OO ONOI MYO WOABNATIVH dOOMNAM

AX 4LW1d

Ris—GeroLtoey oF ORANGE County. 437

abundant remains in certain layers. The rock dips N. 25° W. 10°, and
shows cleavage planes dipping at a high angle to the southeast (1,477 A8
of @,1S. P-.).

Farther up the Neversink valley, a short distance north of Rose Point,
along the west side of the railroad, are coarse blue arenaceous shales, with
sandstones one foot or more in thickness. The dip is 45° W. and the strike
N. 30° H. Fossils are common (1,478 Al of C.S. P.).

Prosser’s most northerly station of Hamilton rocks in the township is
northwest of Cuddebackville and one mile northeast of Rose Point, where
the black argillaceous and arenaceous shales crop out at the base of the
hill. The ledges farther up the hill contain abundant Hamilton fossils (1,478
Bi of C.S. Bo): |

Following the road westward from Huguenot over the hills to Hones:
ville, the following beds were observed.

A short distance west of Huguenot (66) were black indurated shales and
sandstones of Hamilton age, in layers about one inch thick. They strike
N. 40° E. and dip 30° W.

About one mile farther (67), at 700 feet A. T., coarse sandstones, striking
N. 50° E. and dipping 30° ‘W. were met. They are thinly bedded and con-
tain numerous plant stems, as well as fair specimens of Lepidodendron
gaspianum., A mile and one half west of Huguenot, at a bend in the road (69),
and 710 feet A. T., with the strike and dip the same as before, are calcareous
sandstones with an abundance of fossils in certain layers.

The remains are closely packed together. Those determinable were:
Spirifer mucronatus (very common), Spiriter granulifer, Spirifer fimbriatus
(showing the dermal spines), Spirifer audaculus, Leptodesma Rogers, Chonetes,
a small form of © coronatu or syrtalis, Chonetes scitula, Nuculites triqueter
(small form), Spirifer mesastrialis, Leptodesma, sp., Microdon, sp., Trop?-
doleptus, sp.. Phacops rana, Goniophora, sp. Athyris sp. Tropidoleptus
carinatus, Leda diversa, Nuculites oblongatus, Grammysia sp. Lingula, sp.,
Leiorhynchus, sp., plant stems. The plant stems occur in the same layers
with the shells, and concretions are not uncommon. I regard this outcrop
as of Hamilton age.

At the summit of the ridge (70), 1,265 feet A. T., the bluish grey sand-
stones appear and, a little farther on, interbedded red shales which strike
nearly north and south, and dip 20° W. These red shales crop out along the
road through the woods to the west at several points. This region is an

elevated flat-topped ridge covered with a thick growth of scrub- ak,

438 Report OF THE SraTeE GEOLOGIST.

After passing the cross-roads at a small post-office, three miles north of
Sparrowbush, and turning down the valley to the south, there are abundant
exposures of the grey Chemung sandstones. They are well seen in Robert
Coulter’s quarry, north of Sparrowbush, where they strike N. 40° E. and
dip 10 to 20° W. The quarry face is thirty feet high. The rock is a grey
dagey sandstone, heavily bedded in the lower portions of the quarry. Jt
is traversed by numerous joints, whose faces are often lined with quartz
crystals.

The Chemung formation of Deer Park township consists for the most
part of greyish sandstones, which are sometimes thinly bedded. In the
southern portion of the township the boundary is such farther to the west,
and on account of the scarcity of fossils there is some difficulty in fixing
the exact eastern limits.

Prosser gives several Chemung localities in his bulletin on the Devonian
of Eastern New York and Pennsylvania. They are:

A mile east, up the road from Rose Point and below Mr. McCarron’s
house, are thin flaggy sandstones. of a greenish grey color, which contain
Chemung fossils (1,478 A2). Prosser lists several species, and the following
were found by the writer: Zropidoleptus carinatus, Chonetes, sp., Tentacu-
lites, sp.

Near the top of the hill, and north of the road, is Meyer’s quarry (47).
The rock is a bluish grey flagstone, with shaly partings. Fern stems occur
in some of the layers, which dip 18° N. W.

From McCarron’s house up to the school-house, along the same road, are
many outcrops of thin-bedded bluish grey sandstones, with occasional shaly
partings. They strike N. 30° E. and dip 380° W. (46).

About 500 feet north of the schoolhouse is Jackson’s quarry. The
rock is bluish grey Chemung sandstone, with joints running N. 30° E. and
N. 380° W. The layers strike N. 60° E. and dip 25° N. W. About fifteen
feet are exposed in the quarry. The lower beds are thicker and contain
fragmentary plant-remains.

Two miles west of north of Brookville and three miles northeast of
Cuddebackville, is the Ferris quarry, 1,220 feet A.T. The rock is a coarse
grey sandstone, with partings of greenish to olive argillaceous shale. It dips
18 to 20° and 40° W. of N. Prosser considers this to be the same horizon
as the Starucca sandstone.

Below is the section along the Delaware river, from Pond Eddy to Port

Jervis, as measured by White and modified by Prosser :

‘ATNMANSGOW OL GVO SHL NO ‘WOIMYVAA JO LSSM ALVIS YSAIHY NOSANH

IAX 3LV1d

PR ouek

ik? a ath

hi

ini ee

Rizrs—GEoLoGy of OrANGE County. 439

( Délawaret Wags, hy) oe oG 7 "~. 400 feet.
_. | New Milford red shale,. . . . LOO. ~
Chemung with | |
; 4 Starucea; Sandstome;'. 9. 2. 600. «
Portage,. . Cais meg
| Chemung sandstone,.. . .:. 1,150
| Genesee slate, white,. . . . . 200 -
f Fram pomemsraetee ee. 1,400 ©
Hamilton, . . a
WMarcelives 2.09 os 800 «
Upper Helder- ( Corniferous (Onondaga), . . . 200 “
Pau Esopus’. 92. = 2... 2502 «

5,100 feet.
Hupson River Sates anp Sanpstrones. The rocks of this formation
cover such a large portion of Orange county, probably two-thirds of its area,
that they deserve special mention.
In the western portion of the county, im Mount Hope and Greenville
townships, the shales and sandstones form the eastern slope of Shawangunk
mountain, previously mentioned. The beds here exposed are alternating

shales and sandstones, the former having a pronounced cleavage which is not

1

FIGURE 12a. Section across the south end of Sugar Loaf mountain, showing probable fault between
Cambrian limestone, C., and Pre-cambrian gneiss, G. The latter passes unconformably under the
Bellvale flags,

shared by the latter. In the railroad cut, west of Otisyille, the shales dip
40° W. Northeast of Otisville, along the road by Scudder’s house, the sand-
stone members are prominent and strike N. 60°. The region north of Otis-
ville has a heavy covering of stratified drift, but where outcrops occur the dip
is west, while on the southeast side of Shawangunk hill the dip is to the
southeast, indicating a probable anticlinal arch with its axis along the river,
The reddish sandstone and quartzitic members predominate in the region
around Howell’s station. In the cut just west of the station, the sandstones

show a low anticline, and the next cut to the west, exhibits a monoclinal fold.

440 Report oF THE Srare Groots.

Such local foldings are by no means uncommon, The southeast dip, in the
region southeast of Shawangunk hill, changes to a low western one in Mini-
sink and Wawayanda townships, where the slates overlie the Cambrian
limestones. The sandstone beds have disappeared, and the formation is rep-
resented by hard, black slates, with a pronounced cleavage. South of Denton,
the slates give rise to many steep ridges.

From the Wallkill river southeast to Belgrave mountain, there is only a
narrow, wedge-shaped area of slate, which begins west of Sugar Loaf moun-
tain, and extends south as far as Warwick. It rests unconformably on the
Cambrian limestones, and, while the bedding is often obscured by the marked
cleavage, it seems, in general, to be dipping to the west. Glenmere lake lies
just within this slate area.

North of Goshen the sandstone members again appear. and are occasion-
ally fossiliferous. A mile and one-half northeast of Goshen, and just after
crossing the railroad, the slaty members are prominent, striking N. 60° E.,
with a dip of 20° W. The dip is very variable, however, and about 500 feet
farther north it changes to 70° W. The layers here become more siliceous.

A little beyond locality 461, at 472, the sandstone layers have a low
western dip, and contain abundant remains of Ovthis testudinaria and
crinoid stems.

Southwest of Neelytown (464), the slate dips 40° N. W., while north-
east of it (478), the dip is northeast. In general, the slate dips away from
the limestone area at Neelytown.

At the north end of the iron bridge across the Wallkill river, at Mont-
gomery, and in the river bed, are abundant ledges of slate, with occasional
sandstone layers. They here strike east and west and dip 35° N. To the
southwest of Montgomery, however, the strike is generally northeast, with a
western dip.

An examination of these and the other strikes and dips plotted on the
map of this region, indicates that there must be numerous and probably
gentle flexures.

The Wallkill river at Walden flows over a ledge of slate and sandstone
twenty-six feet high, and then through a gorge sixty feet deep, affording fine
exposures of the westwardly dipping shales and sandstones.

Southeast and east of Goshen, the Hudson river slates extend to the
range of gneissic knobs northwest of Skunnemunk mountain, where they
rest unconformably on the gneiss. Their relations have been mentioned in

another part of this report.

‘NB0uy LY Au¥YuYNO ANOLSSINIT

. oe ey

IWAX SLW1d

Rirs—GroLocy oF OrAnGE Counry. 44]

From Walden, the slates and sandstones reach eastward to New Windsor
and Newburgh townships, to the Hudson river. Along the northern border
of the county, the sandstone beds are especially abundant, and conglomerate
layers also appear.

The thickness of the Hudson river formation is difficult to determine on
account of the many folds and the heavy drift covering in that part of the
county where the formation is found. It is probably not less than 1,800 or
2.000 feet. Where it comes in contact with other formations the relations
are invariably those of unconformity, faulting or overthrust. These various
relations are noted in detail elsewhere, and need not be repeated here.

Organic remains. ‘The exact age of these slates has been a matter of
considerable discussion, owing to the apparent scarcity of fossils, Mather*
mentions a locality near Sugar Loaf village, west of the station, and at
Bulmer’s quarry, and states that a few specimens of “testacea” were found
(p. 369). He also mentions another locality near Walden.

In 1885, Darton collected the following species from Bulmer’s quarry :

Orthis pectinella.

Orthis testudinaria.

Orthis plicatella.

Leptwena sericea.

Camarella hemiplicata.

Strophomena alternata.

Streptorhynchus planumbona ov S. filitexta.

Trinucleus concentricus.

Those at Walden are found at the junction of beds of sandstone and
slate below the bridge. The species found were :

Lepteena sericea.

Orthis testudinaria.

Orthis pectinella.

Conularia Trentonensis (? ).

Darton also mentions a new locality in the shales of the railroad cut at
Rock Tavern, where the rocks are bent into an overturned synclinal. The
fossils occur in the lower members, and are not included in the crumple.
The species found were :

Leptwena sericea.

Orthis testudinaria.

= = — Sc jjceo[—_]=

* Geology of New York, Part I., 1843, p. 369.

442 Report oF THE STATE GEOLOGIST.

More recently Professor Prosset has recorded a fossiliferous locality in
the blue-black shales at a cut of the Lehigh and Hudson railroad, one-
quarter of a mile southwest of Greycourt station.

The species found by the writer at the Sugar Loaf locality were :

Orthis testudinaria.

Orthis pectinella.

Leptaena sericea.

Strophomena alternata.

Crinoid stems.

A number of specimens of Orthis testudinaria were found in the shales
about two miles southwest of Oxford (203), and in the Hudson river sand-
stones a mile and one-half northeast of Goshen (472).

Mr. J. N. Weed, of Newburgh, informs me that fossils are abundant in
the sandstones of the point at the south end of Orange lake, and in nearly
all the outcrops of the same members north of Middle Hope.

The fossils found at all these localities indicate a Trenton-Hudson fauna,
as previously stated by C. D. Walcott (Lb. G. S. A., I, 1890, p. 344).

Tue Neetyrown Linestonr. Neelytown is in Hamptonburgh township,
four miles south of Montgomery, and in the woods south of Neelytown station
is a small area of light blue, granular limestone, which is sometimes brecciated
in its upper layers. The limestone first crops out in the cross-road, a few
hundred feet east of Neelytown station (477). A short distance to the south,
on the west side of the road, in a field, is a small limestone quarry (475).
The rock is massive and irregularly bedded, with a brecciated structure, and
very indistinct traces of fossils in its upper layers. Chert nodules are very
abundant. The strike is east and west, the dip north. There are a number
of small outcrops of limestone in the picnic-grove to the southwest, and at
the end of the lane leading into it is a low cliff of the limestone, with the
layers dipping gently to the northeast. In texture, the limestone resembles
closely the upper layers of Lookout mountain, south of Goshen, and is pro-
visionally mapped as of the same age. ‘There is no good evidence that
the limestone was brought up by a fault, and it is probably the crest of a low
anticlinal fold, from which the overlying slates have been eroded.

A careful search was made for other outcrops of limestone between Neely-
town and Walden, but none were found which were clearly in place.
Three small outcrops contaiming Helderberg fossils were found. The first

was southwest of Neelytown (465), another east of Montgomery (474), and

STUW GNVIHSIH 30 1Sv3 'SSIVHS G3Y¥ GOOMONO7T NI ANYYAO

aU JMyyo NoaaNa1WHdOOWNAM,

26

XIX 3LW1d

Rres—GroLocy ofr Oranck Counry. 443

a third just east of Walden (480). They are probably deeply buried
erratics. The strike and dip of the Hudson river formation surrounding the

Neelytown limestone is given on the map.

Geology of Newburgh and New Windsor Townships.

The relations around the northeastern end of Skunnemunk mountain and
Pea hill have already been alluded to. In Newburgh and New Windsor
townships the areal geology is briefly thus: A belt of Cambrian limestone
in the northeastern corner of Newburgh township, with another belt of the
same limestone with some Chazy limestone, west of Newburgh. To the north-
west and southeast of this area are two small gneiss knobs. The rest of the
territory is of Hudson river shale. The Hudson river shales and sandstones,
which cover the western and central portions of Newburgh township, are
faulted against the Cambrian limestone in the northeastern corner of the
township. This fault line crosses the Hudson from Dutchess county, and,
entering Ulster county south of Marlborough, passes southward, entering
Orange county one mile west of the Hudson river. The limestone has a
low western dip, and presents numerous outcrops which form small, rough

ridges.. Owing to the massive character of the rock, the strike and dip are

not always distinct. The line of fault is indicated by a narrow valley, which

extends southwest as far as Middle Hope where the stream occupying the
valley turns abruptly westward. The western boundary of the limestone
extends down to Balmville, and then curves around to the river. The slates
appear to the south of the limestone, but the drift conceals their exact
relations.

There is a small area of Trenton along the river road, between Newburgh
and Roseton, about two and three-quarters miles north of the Newburgh
ferry, and at the point where the road comes in sight of the river. The
Trenton limestone forms a ledge about 300 feet long and twenty to thirty
feet high, on the west side of the road (879). The dark crystalline limestone
has a strike of N. 35° E. and dips 40° E. The ledge is about 135 feet above
the river. The limestone contains a mass of small encrinal columns and
small Cheetetes. The crinoid present in especial abundance is Cleiocrinus
magnificus, a® species which had only been previously found in Canada
until its discovery by Professor W. B. Dwight at this locality.* There
are also several other species of Trenton age, viz.: Platystrophia lyna,
Plectambonites, ete.

* A. J.S. (3), XTX., p. 50.

444 Report oF THE STATE GEOLOGIST.

One-half mile to the north is an outcrop of shale along the roadside by
an old barn. It occupies a small triangular area. Above it on the hill the
Cambrian limestone appears, as well as to the north of it in a quarry by Mr.
Rose’s house. At this latter locality the dip is to the southeast. The exact
relations are here again obscured by the drift, but the Trenton may rest on
the Cambrian, and the Hudson river shales may rest either on the buried
Trenton or directly on the Cambrian, by thinning out of the Trenton or by
faulting.

To the southwest of Balmville, which is on the northern edge of
Newburgh, the limestone again begins and extends, as an elliptical area of
four miles in length, in a southwest direction to Washington lake. The
width of the area is about one mile and a quarter. To the northwest it rests
on the Olenellus quartzite, and this in turn on the gneiss of Cronomer’s hill.
The rest of the distance it is overlaid by the Hudson river slates. On the
southeast, the limestone dips in part under the slates, and is faulted against
the steep northwestern side of Snake hill. The dip of the limestone is
generally southeast. There is doubt whether all of the limestone of this area
is of the same age. Over the larger portion of the area it is a crystalline,
cherty limestone, very much resembling that of the other Cambrian areas,
but in the southeastern part, in Miller’s quarry, the rock is more evenly bedded,
and less massive.

Some years ago Professor R. P. Whitfield published the discovery of
probable Maclureas in parts of the limestone. This indicates the Chazy age
of a portion of the limestone, the greater part of which is probably Potsdam,
accordiug to an opinion expressed to the writer by Professor Dwight (See
also, A. JS, iii, XVIIL, 327, 1879). The specimens were fragmentary, and
none have since been found. Professor W. B. Dwight informs the writer
that he has found a few ill-defined Calciferous fossils in the limestone of
this area northeast of Washington lake.

Southeast of Washington square, the Hudson river slates extend around
the south end of the lmestone area and rest uncomformably against the
gneiss at the south end of Snake hill. The slate crops out along the road at
the southern end of the hill (407a), and extends along the east side of it,
appearing at several points, and especially on Mr, Hasbrouck’s race-track,
where it has a strike of N. 40° E. and dips west. Farther south along the
road, the dip is east. The slate is also seen at the north end of Snake hill,
at 215 feet A. T., along the road leading to the pavilion on the summit, and

along the road by the ice-house at the northwest base of Snake hill. The

‘ATMASILO SO LSSM LAND avouTivy NI S3LVIS Y3SAId NOSGNH GNV BLVYSWOIDNOD VAOISBNO NS3SML3S ALINYOSNOON()

XX SLW1d

e . ,
* ‘ *

. Ly : «

bad , e 7

‘ | “ ¢
; I
1 ce
¥
' ee ®
. i ‘
‘ j 5%
ii 4 ;
= ' t

¥ (

Ries—Gurowiocy. oF ORANGE County. AAD

limestone crops out on the same road to the south of the slate, as well as
on the opposite side of the ice pond. The fault between the gneiss and
limestone on the west side of the hill seems to pass to the north between
the latter and the slate, or may die out.

The gneiss of both Cronomer’s hill and Snake hill is a granular mixture
of quartz and feldspar, with little or no mica. In a small gneiss area south
of Snake hill the rock is often graphitic.

The Hudson river slates extend to the foot of the mountain between
Mountainville and Cornwall, and are possibly faulted against the gneisses of
the Highlands. ‘The two can be seen close together at several points about
one mile and a half south by east of Canterbury, the slate apparently dipping
under the gneisses (420). The gneiss strikes N. 30° E., and dips southeast.

One-half mile south of Cornwall (421) is an old road-metal quarry in
limestone. It is a dark grey, finely crystalline rock, striking N. 80° E., and
dippmg 45° $8. There are interbedded grey brown, siliceous layers, and
numerous black patches of carbonaceous matter along the bedding planes.

The limestone passes under the slates and probably belongs to the
Olenellus quartzite, certain members of which it resembles very closely.
About twenty-five feet of limestone are exposed (422). The dipping of the

quartzite against the Pre-cambrian gneiss would at first suggest a fault,
but it may be the southern side of a fold caused by the quartzite being thrust
against the gneiss. This, Professor Dwight informs me, is sometimes the case
in Dutchess county. The slate and gneiss are seen almost in contact a few
feet east of the quarry.

The writer mentioned this limestone quarry to Professor Dwight, who
has done much field work in the neighboring counties, and he has written in
reply: “In 1883, I found that there is a thin stratum of impure, hard lime-
stone overlying the gneiss, and underlying the Hudson river shale along
the northern and northeastern base of Storm King and south of Cornwall.

“This occurs, as I then ascertained and noted, on the estate of Mr. S. B.
Young, whose house is at the northeastern base of the mountain, south of
Cornwall. This stratum of limestone was encountered in making excavations
for the cellar of his house, and for his ice-house. Blocks of the excavated
limestone lie around, and some of them were built into the walls forming the
approach to the ice-house.”

Further on in his letter, Professor Dwight says, in referring to the
quarry: “I take the limestone in question at Cornwall to be the Lower
Cambrian limestone (Olenellus horizon).”

446 Report oF THE State GEOLOGIST.

Tue Higuranp Arra or Gyetsstc Rocks. The following notes on the
Highland region are to be considered as merely preliminary and in the nature
of a reconnaissance. The crystalline rocks of this region present a most
interesting field for study, and it is hoped that opportunity will be afforded for
a further and more detailed consideration of their relations. Such detailed
work requires a most careful examination of all the outcrops and careful petro-
graphic examination with the microscope. Considerable has been published
hereupon in the report of Mather,* and certain portions of his work will be
referred to further on. Britton and Merrill also refer frequently to these
rocks in connection with their work on the Highland area in New Jersey.+

Excluding the areas of gneiss forming the western half of Pochuck
mountain and another strip along the northwestern side of Bellvale mountain,
the gneissic rocks cover all of the townships of Tuxedo and Highland, and
about one-half each of those of Monroe, Woodbury and Cornwall.

Tuxrepo Townsuip. The gneiss rises steeply along the eastern side of
Greenwood lake with a dip of 60° E. It is often massive, and sometimes
much shattered by joints at right angles to the stratification. These joints
not uncommonly represent fault planes. The gneiss is a mixture of quartz,
red orthoclase and hornblende. Specimens of this same gneiss, collected
from a point on the New York and New Jersey state line, were examined by
Professor Kemp in 1885 (NV. -/. Geol. Surv., 1886, p. 102), and the orthoclase
found to be full of curious little inclusions.

Northeast of Greenwood lake, the gneiss is strongly laminated and is com-
posed of biotite, feldspar and much quartz. The region between Greenwood
and Sterling lakes is heavily wooded and has not yet been examined. On
its eastern edge the rock along the shore of Sterling lake (346) is a dark-
colored, fine-grained basic gneiss. A section of the fine-grained portion of
this gneiss, from half way up the west side of the lake, shows it to consist of
plagioclase, hypersthene and magnetite. The plagioclase is in large plates,
fresh, and full of beautiful apatite crystals. The hypersthene is strongly
pleochroic and the magnetite grains associated with it are large and rounded.
The dark, massive gneiss, one and one-half miles north of Sterling lake, may
be a continuation of this area (801). Sections of it afford much microperthite
and some quartz.

The dark hornblendic gneiss surrounds most of Sterling lake and contains

oD

the ore-bodies at the southeastern end of the lake. At this point are two

* Geology of New York, First District, 1842.
+ Geological Survey of New Jersey, 1885.

‘SNIW TISNO WOYS ! SLILANODVI HLIM BLIOIWD “€| BYNOI4

1409.0405MV 49 HOISN

STAVH.dOOUNAM,

+o

‘

44

County.

ORANGE

1
(FEOLOGY OF

Ries

‘O10 919 SULULUL UL paMo][OF poyjeur pue A, Oq-a10 JO GUI[JNO BUIMOYS ! sosulul eyLTT PUB Suljleyg Youoiyy uUoloosg

ayo
Suider

N

~~ Qa

SUI, 24D7

evar

,00Z

SUITAl buij4eic¢

‘PL aun”

448 Report oF THE SrateE GEOLOGIST.

beds of magnetite, the Sterling and the Lake. They are evidently portions
of the same bed cut in two by a pinch. The direction of their longer axes
is about northwest and southeast, and this strike carries the Lake ore-body
beneath Sterling lake. The length of the Sterling ore-body at the surface is
500 feet, and 230 feet at the bottom of the workings. The length along the
slope, which runs obliquely down the dip, is 1,000 feet. The pinch is about
250 feet long and is succeeded by the Lake ore-bed, whose outcrop is of the
same length, but its depth is not known, as it has never been fully exploited.
The slope is 1,100 feet long.

The ore-bed varies in width from five to twelve feet and is sharply
defined. The ore formerly extended up the surface of the hill at whose base
the entrance to the present workings is situated, and quarrying methods were
therefore employed for operating this upper portion of the ore-bed. In a few
places on the face of the hill where the hanging wall remained, as in the
Clark mine, chamber-working was followed. The Clark ore-body dips to the
northeast, and swells and pinches in a remarkable manner. At one place
in the footwall, two narrow anticlines have been produced, as shown in
Figure 15.

The wall rock is a basic gneiss, with much hornblende, and the roof
of the chamber-working is a very coarse-grained mixture of plagioclase feld-
spar and hornblende. Just above the ore at the northwest end of the open
working is a feldspar vein, twelve inches thick, which extends for about
twelve feet and then suddenly pinches out. Veins of epidote and milky
quartz crystals occur in the wall rock and frequently cut across the strike.
The gneiss around the ore-body contains less hornblende than that farther
down the hill towards the Lake mine.

The Lake mine has afforded quite a variety of minerals which occur on
the edge of the magnetite bed. The commonest are pyroxene and amphibole
either in distinct crystals or forming granular aggregates with the magnetite.
At other times there is present in these granular mixtures both white and red
feldspar, the former surrounding the latter. Clusters of small epidote crystals
are seen, usually in association with pyroxene. Some beautiful pegmatitic
intergrowths of quartz and tourmaline are found in the Lake mine, but in
just what part of it, the writer was unable to ascertain. Sometimes this
intergrowth is surrounded by red feldspar, and the latter encircled by mag-
netite. On the hill and along the highroad about 500 feet northeast of the
Lake mine, are several small lenses of magnetite in the gneiss. The stringer

is lens-shaped and near the outer margins contains some granular quartz.

ro)

*ISSMHLYON SHL OL SdIQ YOON SHI ‘STINASILO SO LSSM AXYVNO NI LIND YNNONVYMVHS

pA ae ig oe Py Fx ouosnwss 103 aN azamsTOON LEM!

Pi and

is
is

ak

A
.
ye
4

|

5 ee

IXX SLW1d

Rizrs—GEOLOGY OF URANGE Counry. 449

The wall rock is feldspathic and has no hornblende, as indicated by the light
color which it has in the figure.

From the Sterling mine the basic gneiss continues northeastward towards
the Augusta mine which is also on the property of the Sterling Iron and
Railway Co, The strike of the gneiss at this mine is N. 40° E. and the dip
50° KE. The rock is made up of alternating bands of feldspar and hornblende
and the ore seems to favor the latter, dipping with the rocks. According to
the sections drawn from a survey made several years ago, the ore-body is long
and flat. There is a notable fault exposed in the hanging wall at the

entrance to the.mine. The layers of the gneiss have been drawn down by

100'

FIGURE 15. Diz ic view ark mi Sterli i
URE 15. Diagrammatic view of Clark mine, at Sterling; showing swelling and pinching of the

ore-bed. The section is N. W. and S. E. Cisavein of feldspar and hornblende, one foot thick
which is pinched out. Bisa N. E. and S. W. section of foot-wall at A. é

the shearing action of the faulting. The foot-wall of the Augusta mine
contains much granular dark green pyroxene. ‘There are many coarsely
crystalline veins of quartz and feldspar which cut the gneiss in the walls
; er a ; ;

of the Augusta mine. They not uncommonly cut directly across the strike
and are often branched.

rity . . . ry .

The Mountain mine is about three-quarters of a mile north of the fore-
going, and consists of several long narrow parallel beds. At the Scott mine,

the gneiss is more acid and contains little or no hornblende, not even in
29

450 Report or THE Svrare GEOLOGIST.

the walls of the ore-body. Orthoclase feldspar abounds. The rocks around
the ore-bed have been much sheared and strained, but no actual faults were
found on the surface. One of the specimens showed a breccia of feldspar
and magnetite. One mile northeast of the Oregon mine, the grey gneiss
again appears, being a mixture of quartz, feldspar and biotite. It dips 40° E.

Along the road leading from Greenwood lake to Tuxedo and in the area
due north of Sterling lake, the gneiss is, at times, very massive, with red
feldspar, and resembles granite. Just northeast of the cross-roads, on the
road to Southfield (305), the rock is a massive, red, feldspathic gneiss with
some quartz and much garnet. It strikes N. 20° E. and, dips 70° 8S. E.
Little or no mica is present.

This may be only a local variation, for about a mile and one-half farther
to the north the common grey gneiss again appears, striking N, 25° KE. and
dipping 40° EK. The strike is, however, very variable.

From Southfield Works to Helmsburg, south of Mount Basha lake, the
gneiss preserves a remarkably constant character. It is fine-grained, light
erey, strongly laminated and composed of quartz, orthoclase feldspar and
biotite. Some plagioclase is present, and hornblende is not uncommon. The
strike near Southfield Works is N. 40° E., dip 60° S. E. Farther to the east,
along the road, it is N. 20° E., dip 60° S. EH. At this point the gneiss
sometimes contains dark bands of more basic rock, which in appearance
resembles the gneiss around Sterling lake.

Much of the gneiss m Tuxedo park is fine-grained and very basic, that at
the southern end of the park, especially, containing considerable quantities of
pyroxene, with strong basal parting. The dip is nearly always to the east.
Along the Switchback road, near the summit of the hill and at a point about
330 feet higher than Tuxedo station, there are numerous veins of a coarse red
granite identical with that found near Stockbridge’s hotel, east of Central
Valley.

On the cireuit road within Tuxedo park there are many exposures of a
well banded grey gneiss with alternating light bands of quartz and feldspar
and dark ones of hornblende, with some biotite. The gneiss strikes N. 40°
E. and dips 50° 8. E.

One mile before reaching the north gate and on the circuit road, are

large outcrops of an extremely coarse dioritic rock, similar to one southeast of

oo
g
Southfield. It is much coarser, however, and contains some quartz. In close
association with it is a fine-grained granular gneiss and stringers of the diorite

often penetrate Life

‘ONITHSLS YVAN ‘SSIBND NI SLILANOVW 4SO SNA] '9) SYNSDI4

GEOLOGY OF ORANGE CouNTY. 451

Ries

Mather refers to a cliff of limestone one-quarter of a mile southwest of
Tuxedo lake, and states that it is traversed by a faulted dike. A search was
made for this outcrop at the point indicated by Mather, but the writer was
unable to find it. Quartzose gneiss forms a steep and possible fault cliff in
the road-metal quarry south of Southfield, striking N. 40° E. and dip 70° E.

One mile south of Southfield, along the road through the woods, 1s an
area of very coarse diorite. The rock is a coarse mixture of labradorite and
hornblende, and shows well the crushing which it has undergone. This same
rock also crops out in the field along the upper side of the road, until the
latter begins to curve around the hill, when it is succeeded by a massive
gneiss, with quartz orthoclase and biotite. This gneiss becomes very coarse
in places, when the biotite is replaced by hornblende. It continues with
somewhat variable character to Little Long pond, with a strike that varies
from N. 20 to 50° E. and a prevailing steep eastern dip. At the west end of
this pond, the gneiss strikes N. 20° E. and dips 30° E., while at the east end it
dips 80 to 90° EK. Along the road leading up the hill west of the pond, is a
pegmatite vein cutting the gneiss, and this latter is cut by five camptonite
dikes in a space of 200 feet. They may be possibly branches of the same
dike. They vary im width from two inches to one foot.

Monror Townsuie. The gneisses cover nearly one-half of the township,
their western border being along the eastern side of the valley, extending
from Greenwood lake to Monroe.

East and northeast of Long pond, which is two and one-half miles south
of Monroe, the normal grey gneiss is composed of orthoclase, quartz and
biotite, with subordinate hornblende. The rock sometimes becomes coarsely
crystalline, with an increase of the hornblende, and this passes into the
normal facies again. Southeast of Long pond, and on the crest of the ridge,
the strike is N. 20° E., dip 70° W. A common form of the gneiss in this
region is a red rock consisting of quartz, orthoclase, plagioclase and some
biotite. The plagioclase frequently exceeds the orthoclase in amount. The
quartz commonly has a zonal structure and contains apatite and zircon as
inclusions.

In the region south of the Clove mine the grey gneiss is generally
quartzose, with few variations. On the eastern side of Mount Basha lake it
becomes garnetiferous.

The O'Neil mine is three miles southeast of Monroe. It is a large
opening about 200 feet west of the road, and below it. The pit is about fifty

feet deep and 600 feet long, extending northeast and southwest. The wall

452 ReEpoRT OF THE STATE GEOLOGIST.

rock is a coarse feldspathic gneiss, that on the north wall being somewhat
more quartzose. The rock strikes N. 30° E. Near the west end of the main
cut is an olivine camptonite dike six feet wide, which cuts across the ore-
body. The ore was mined out around it and the dike has been left standing
like a wall. Another dike of the same rock, or a branch of the first one, is
found in the next pit, about 200 feet to the southwest. Just west of the first
dike, and next to it, is a coarsely crystalline rock of granitic structure (shown
in upper left hand portion of the adjoining figure), and consisting of feldspar
and serpentine; the latter, however, is evidently an alteration product
of either pyroxene or hornblende, perhaps the latter, as Mather records a
syenite rock penetrating the ore-body.

Next to the ore, the wall rock becomes very basic, and contains a mixture
of magnetite and pyroxene, or hornblende. In places, the latter has changed
almost completely to serpentine, as in the northwest wall just east of the
dike. In the pit where the second dike occurs, the rock, on the north side is
an altered syenite, but next to this second dike the rock is a mixture of
calcite, with hornblende or magnetite. Lying in the pit are several masses of
calcite, filled with a reticulation of magnetite streaks. Just what part of the
mine this came from could not be determined, but the occurrence of it in this
large quantity is somewhat suggestive of a possible sedimentary origin.

The wall rock is traversed by many joints, and the great masses of rock
which have fallen into the pit obscure the relations considerably. Two
chambers have been driven at the eastern end of the pit. The mine has not
been worked for sixteen years. Probably no locality in the county except
Edenville has afforded so many minerals. The most abundant are beautiful
little octahedral crystals of magnetite. Pyroxene and amphibole crystals
have also been found.

A list of the minerals which this mine has afforded is given in Mather’s
report on the Geology of New York, First District.

The Forshee mines are on a neighboring hill about one-half mile south-
west of the O'Neil mine. The main working is an open pit, about 400 feet
long, fifty feet wide and fifty feet deep. The country rock is a feldspathic
gneiss striking N. 20° E., and dipping 40° S. E. The ore is very lean and
associated with a peculiar pyroxenic rock with a bronze lustre. It very
strongly resembles enstatite, but sections of it give an inclined extinction.
The rock is very hard and rather coarse-grained. It is traversed in places
by quartz veins. The rock at and around the base of the hill is the

ordinary grey gneiss.

ONIWHYSLS YVAN ‘SOVNYNSA AYYNOILNIOASY A190 ‘LI B3yundl4

-09.G404MV¥YH9O XOS8N371VH DOOWNAM

Rirs—Gronocy oF ORANGE County. 453

The Clove mine is about a mile and one-half south of Monroe. The
workings are full of water and little of their relations can be made out.
According to Mather* the ore occurs in several parallel veins. This may be
due to faulting. The walls of the mine are a hornblendic gneiss which, at
times, becomes very schistose, and the ore has much hornblende and a
silvery mica mixed with it. Pyrite is occasionally present. The nearest
gneiss exposure to the east of the mine is very quartzose and does not
represent the normal rock. On the west are several outcrops of a feldspathic
granitic gneiss. The ore-body is evidently cut by a dike, judging from the
numerous angular fragments of it which were found on the dump heap. The
dike is a fine-grained black rock, cut by numerous thread-like streaks of
pyrrhotite.

Woopsury Townsuir. The gneissic rocks cover about five-eighths of
the area of the township. The line of faulting which has given rise to the
Ramapo valley south of Turners, passes northward along the base of the
gneiss ridge east of Turners and Central Valley, and then along the narrow
valley east of Pine hill, at whose north end the fault-line probably passes into
the Highlands. Up to the point east of the north end of Pine hill, the fault
line is between the gneiss and the Cambrian limestone. A contact of the two
is well exposed in the limestone quarry a mile and one-half northeast of
Arden. <A fine fault cliff is also to be seen on the western side of the valley
just north of Arden. The grey gneiss, which is faulted against the limestone
in the upper portion of the limestone quarry, dips steeply to the east. It is
a fine-grained granular mixture of quartz and plagioclase with a little
orthoclase and biotite. The rock shows the effect of crushing, and the larger
grains are embedded in a crushed matrix of the same minerals cemented
with decomposed biotite and limonite.

About one mile below the quarry, a road leaves the main one of the
valley and turns to the east through a shallow ascending valley to the other
side of the ridge where it turns to the north. Just beyond a church and
where the road turns, a granular gneiss appears, which is cut by numerous
granite veins. It strikes N. 20° E., and dips 70° S. E. (284). The gneiss in
section is seen to consist of quartz, plagioclase and some orthoclase. The
quartz grains often show a zonal structure, and the twin lamellae of the
plagioclase are not unfrequently bent. The rock is considerably decomposed.
This gneiss passes into a very hornblendic facies.

* Geology of New York, 1842, p. 571.

454 Report oF THE STATE GEOLOGIST.

About one-quarter of a mile beyond Mr. Harriman’s house, the gneiss
becomes very quartzose and shows many crumples and slickensides. It is a
mixture of plagioclase, biotite, and pyroxene. The two latter occur as parallel
growths and the same cracks traverse both minerals. Another specimen of the
same gneiss from farther up the road (281), shows, in sections, a similar
character but the pyroxene is often nearly colorless and much corroded, while
magnetite is present in small amounts. The strike is N. 40° E., the dip
45° N. E. The gneiss once again becomes dark-colored, very massive, and
hornblendic and is cut by an east and west dike about one foot wide. The
rock on either side of the dike is broken by many joints running parallel to
the dike, and the gneiss strikes N. and 8. with a dip of 60° E. The gneiss
again passes into the normal form along the road above the waterfall. It
will be thus seen that there are alternations of the normal gneiss and the
hornblendic form.

At Mr. Cunningham’s house, about a mile and one-half up the road from
Mr, Harriman’s, the road branches off to the east. Just behind Mr. Cunning-
ham’s, the gneiss contains a small bed of iron-ore. A small. pit was
sunk in it to a depth of nearly forty feet and a little ore taken out, but
most of it was very lean, Across the road to the north a small dike cuts
the gneiss.

About a mile farther east, are several more small iron mines south of the
road. They are the Greenwood, Hogencamp, and Tompkins mines. The
wall-rock of each is a hornblendic gneiss with some granular pyroxene.
The largest mines in this region are the Bradley mines, one and one-half miles
north-east of Cunningham’s house, and on the road to Queensboro, Judging
from the size of the opening, a large amount of ore has been taken out. The
ore crops out above the road and a cut was made to intersect it at a lower
level. The bed of magnetite dips to the north and is fully forty feet thick.
Associated with the ore are great quantities of calcite containing crystals of
magnetite, apatite, pyroxene, titanite, amphibole, and grains of pyrite. Two
dikes also cut the ore-body, one a porphyritic camptonite, the other a fine-
grained quartz porphyry. This latter is a new one to the Highland region of
Orange county. They are both hereafter described in further detail.

From Cunningham’s house to Two Ponds, the road leads through the
woods and there are few outcrops. Where these are found, the rock is
generally a massive gneiss dipping to the east and striking from N, 20° E. to
N. 40° E. Ata point where the road swings around to the west, Just before

passing between Two Ponds, the gneiss is cut by a dike which may be an

FiGuRE 18. CAMPTONITE DIKE, NORTHEAST OF ARDEN

Rizs—GeroLocy oF ORANGE Counry. 455

offshoot of the large knob penetrating the gneiss south of the road. This
rock was found to be much decomposed in the sections examined, but is
probably a camptonite. In front of Stockbridge’s hotel, east of Central
Valley, the gneiss strikes N. 40° E. and dips 80° 8. EK. From the road crossing
the mountain just north of Stockbridge’s, up to the next road across the
mountain, about two miles further, the gneiss is cut by many veins of coarsely
crystalline red granite. This is a mixture of bright red feldspar, large flakes
of biotite and a little quartz. One of these veins crops out along the road
opposite the entrance to Stockbridge’s lane.

The gneiss ridge north of Stockbridge’s, judging from a number of
strikes and dips taken, is apparently a synclinal fold. On the eastern side of
the valley east of this ridge, and about one and one-half miles north of
Stockbridge’s, there is, along the road, a ledge of rock, which in many respects
resembles the contact zones at Mounts Adam and Eve, in Warwick township.
In the lower portion of the ledge and a few feet above the road, the rock is a
coarse-grained mixture of pyroxene, scapolite and feldspar, with some quartz
and calcite. Where cavities exist in the rock, good crystals of pyroxene
are not uncommonly developed, but terminations are rare. The feldspar is

most abundant at the northern end of the exposure and higher up the slope.

55

Up this slope the rock becomes a coarsely crystalline aggregate of feldspar
‘and pyroxene, the former predominating. Some quartz is present. No good
bedding was noticed except in the ledge a few feet above the road, where
there seems to be a low dip to the east. The rock on the west side of the
road across the brook, is a hornblendic gneiss which, in the bed of the stream,
is cut by two dikes, one four inches wide, the other six feet; they are both
camptonites. The exact relations of this scapolite-pyroxene zone and. its
significance require further examination before they can be explained. It is
possible that this may represent a contact zone between a probable granite
rock to the southeast and the hornblende gneiss, or a limestone which
has been removed by erosion or faulted out of place. There is a short belt
of limestone about a mile to the north in this valley, but no outcrops of
limestone were found between these two points. The limestone belt
mentioned thins out at its southern end.

At the south end of Popolopen pond, is a small bed of limestone forming
a natural bridge. It is a bed about forty feet wide and has a length of about
four hundred feet from the south end of the lake to its southern extremity
where it disappears under the meadow. The limestone is interbedded with

coarse-grained gneiss which strikes N. 50° E., and dips 70° E. on the western

456 XEPORT OF THE STATE GEOLOGIST.

side of the limestone. The latter shows no distinct bedding planes, but the
lines of minerals, especially the serpentine, strike about N. 35° E. Scattered
through the limestone are bunches of the ferro-magnesian minerals, pyroxene,
mica and hornblende. They form a dark strip several feet wide on the
western boundary of the limestone at the north end of the bridge. At the
south end and just behind a small barn, the gneiss contains an abundance of
magnetite in grains and lumps up to an inch in diameter. The gneiss on the
eastern side of the limestone contains much pyroxene along the contact and
is distinctly laminated, but farther to the east in the field it contains many
coarsely crystalline granite veins.

Around the Forest-of-Dean mine and the adjoining reservoir, the gneiss
is a mixture of quartz, feldspar, hornblende and biotite, the two latter in
variable proportion. The gneiss dips southeast and pitches about 22° to
the northeast. The ore-body is described under the economic division of
this report. The ore-bed is cut by a camptonite dike and two others occur
along the road to the southwest by the reservoir.

Hicuranp Townsutp. The gneisses of this township are often quite
massive. Along the Hudson river the prevailing grey gneiss is composed
of quartz, orthoclase and biotite. A little plagioclase is present, and the
quartz often contains cavities. The general strike is from N. 40° to 80° E,,
and the dip generally to the east. Pegmatite veins are common and form a
prominent feature of the gneiss. They usually run parallel to the bedding
of the gneiss, rarely cutting across it, and they also commonly partake of the
folding or other distortion which the gneiss has undergone, while their
boundaries are not always sharply defined. On the road from Cranstons
to Fort Montgomery and a short distance north of the latter are several
outcrops of graphite schist; it also occurs in the woods to the west and about
one and one-half miles southwest of the village of Fort Montgomery, along
the road to the Forest-of-Dean mine. In all of these exposures the rock
is much decomposed and stained from the disintegration of pyrite. The
eneiss is very basic south of Little Long pond, and is intersected by several
dikes.

CornwatL Townsnip. The gneisses form the southern half of the
township, extending from Mountainville around the base of the mountain to
Cornwall-on-Hudson, They vary from massive to a bedded variety, and are
normally a mixture of quartz, feldspar and biotite, but sometimes contain
hornblende in great abundance. Towards Cornwall they become very

quartzose and are seen in contact with the Hudson slates along a fault line.

4

WYNKOOP HALLENBECK CRAWFORDCD,

FIGURE 19, WATERFALL NORTHEAST OF ARDEN.

J
a A hell :

©

yoo
» ©

Rirs—Gronocy or Orancar County. 457

Dike Rocks. The only detailed account hitherto published of dikes
from the Highland area in Orange county, are two papers by Professor
Kemp which appeared im 1888*, both treating of camptonite dikes, which
at that time were thought to be comparatively rare rocks. The first of these
is a camptonite from the north end of the first railroad cut above Fort Mont-
gomery. It is a dense black rock, and the dike extends twenty feet or more
vertically, running diagonally across the lamination of the gneiss. Under
the microscope the rock consists of small, well developed hornblende crystals
with sharp faces. There is some plagioclase and a few grains of magnetite,
and the dike has a more or less porphyritic structure. Duplicate analyses
of this rock, which are of value, were made by Professor Dennis*, of Cornell

University. They show:

a. b.
I we ee. 44.85 44,87
PU ey ee 17.20 17.281
I eg a 11.20 11.04
eee Re. trace trace
6.578 6.738
IG OI Ser 3 7.4
Oc ew es BOD 4.946
Pg See, Rb ef es ms 91999 2.621
OM ee A 1.890 1.6
erM ee ely» 888 AAT
ReOUEEe ey ta, —— —
eememromiiom 8 a 9.887 2.491

99.52 99.585

There are no dikes between Fort Montgomery and Crow’s Nest mountain,

but extending up the face of the latter are six dikes which have been noted

_by Professor Kemp. They are holocrystalline aggregates of hornblende,

augite and plagioclase with subordinate magnetite, apatite and biotite, and
e fan) ro) ? i
sometimes orthoclase and quartz.+

The hornblende and augite are generally associated, but may occur singly;

the augite especially in spots where the dynamic action has been greatest.

* A Diorite Dike at the Forest-of-Dean mine, Orange county, N. Y.—A. J. 8. (3), xxxv p. 331 and
The Dikes of the Hudson River Highlands— Amer. Nat. xxii p. 691.
+ For a review of other occurrences of camptonitic rocks and their classification, see Bull. 107, U. S. G. S.—The Dikes of Lake
Champlain by. J. F. Kemp and Y, F. Marsters.

458 Report oF THE STATE GEOLOGIS?.

The hornblende is brown and in irregular masses, with magnetite and apatite
inclusions. It is often bleached to a green variety. The augite contains the
same inclusions as the hornblende. The feldspar is well twinned, and
inclusions of magnetite and apatite are not uncommon.

Another camptonite dike has been described by Professor Kemp from
the Forest-of-Dean mine. The dike is about six feet wide and cuts across the
ore-body at an acute angle. It consists of plagioclase, hornblende and
magnetite, with alterations of the first two. Secondary magnetite also occurs.

An analysis gave:

Si Og ct] SA Oc Ba ee te wee etae nee a eo
Aly Ota aaa ie Rea a cee
Fle, Oo. «tse tempest. ge ie eee ime
CaO. Spee 2. os regen ete eke os eee 6.59

Me Ou pephek) - , Ce ee ee
Ky Ops saa eM E oS 5 Se a eee

Na, O02. 2 SERS Se ee eee ae
Loss on ignition suey Boeke aoe Ae TOR, Cs oe Oreil
100.53

These two dikes are the only ones from the Orange county Highlands
which have been described in detail.

The writer, during his field work this summer, found several other
camptonite dikes in this region, which are very similar to each other and to
those described by Professor Kemp.

One of these is at the turn of the road, south of the Forest-of-Dean mine,
near the east end of the reservoir pond. The dike is six feet wide and extends
east and west through the biotite gneiss. The latter strikes N. 10° E., and
dips 50° E. The dike rock is light grey and has minute acicular hornblende
crystals which are visible in hand specimens. Sections of the dike show it to
consist of hornblende on plagioclase, both much decomposed. The horn-
blende needles and shreds he with their longer axes parallel, Another dike
cuts the gneiss at the west end of the pond. It is almost under the bridge
crossing the creek at this point. This, however, is an olivine-augite camptonite.
The section of this rock shows granular pyroxene, lath-shaped plagioclase and
magnetite grains in the ground-mass, with phenocrysts of olivine. There is
also some glassy material in the ground-mass. The olivine is altered to
serpentine along the cracks and around the edges, with the development of

curiously shaped magnetite grains.

'STIUIW GNVIHDIH AO LSVvA ‘ALINVYD Gay JO SNIBA HLIM SSIFN5 ‘0% AYN!

Pa em OD.GHOGNW US aSENS YF AOONAM

Fl oes ‘eee

Rirs—Gerorocy oF OrANGE Counry. 459

A fine example of a camptonite dike occurs in the Bradley mines, north-
east of Arden, and in Monroe township. ‘The rock is composed of plagioclase
and hornblende, with some magnetite. The plagioclase is altered to a serpen-
tine-like granular material. The hornblende is brown, strongly pleochroic

and idiomorphie, in lath-shaped individuals or six-sided sections showing pris-

eiss

Section of Forest of Dean Ore body

Var = Ve yan Vm v-eveve-

|e PS VS
a A

“Wr Ve Vevey nv —v

Vas
Y= v= ~Dike ea ee Gneiss

=< Yi
Vv At Aol Mell ai All Ae Va

Plan of Forest of Dean Ore body

FIGURE 21.

matic and orthopinacoid faces. There are also large porphyritic hornblendes,
which commonly show zonal structure and twinning parallel to » P x.
Two more camptonite dikes cut the granitic gneiss about one mile (512),
and a mile and one-half east of Stockbridge’s hotel, which is on the mountain
east of Central Valley. They are both much finer grained than the preceding,
and contain numerous round or square grains of magnetite. The feldspar
is much decomposed. The first of these two dikes (512) is interesting on

account of the manner in which it branches and incloses some of the wall-

460 Report OF THE StTaTE GEOLOGIST.

rock. The second also branches, and is about two feet wide. It cuts both
the gneiss and a granite vein. The gneiss strikes N. 45° E., and dips
60 to 70° E.

In the bed of the stream along the road, at a point about one-half mile
north of the cross-road coming over the mountain from Highland Mills to
Forest. of-Dean, are two additional camptonite dikes, cutting the gneiss parallel
to each other. The one is four inches wide and contains phenocrysts of horn-
blende a sixteenth of an inch in diameter; the other is six feet wide and

contains none, Sections show plagioclase, hornblende and magnetite of the

bo
to

FIGURE Dike of camptonite, C., cutting a granitic gneiss, G., one mile east of Stockbridge’s hotel,

near Central Valley, and showing inclusion of the wall-rock.
habit common to this class of rocks. The large hornblendes of the first
generation are both zonal and twinned. These dikes are close to the curious
pyroxene-scapolite ridge of rock.

“Still other dikes of this kind occur north of the Forest-of-Dean mine,
and at a point along the road south of Little Long pond, also about two
miles east of the mine.

The great abundance of these dikes in this region and their constantly

close similarity suggest very forcibly a common derivation, but whether the

PLATE XXII

o
°
rey
ce
So
re
=.
&
yy Be
o
x
oO
w
a
z
Ww

WYNKOOP HALL.

QUARRY IN PENTAMERUS LIMESTONE, SOUTHWEST OF OTISVILLE.

Rirs—GroLtocy oF ORANGE County. 461

parent mass is exposed anywhere, the writer is unable to say, as, in the time
at his disposal, he was unable to examine the Highland region in sufficient
detail.

The distribution of the dikes is not confined to the area of Highland or
northwestern Woodbury townships. A narrow porphyritic camptonite dike
cuts the gneiss northwest of Arden, along the road from Arden to the O’Neil
mine (490).

At the west end of Little Long pond southeast of Southfield, is a curious
little group of five such dikes, which may be branches of the same
dike. These do not penetrate the gneiss to any extent, but are mostly

in a pegmatite vein which cuts it. They are all composed of idiomorphic

FiGURE 23. Section of hypersthene-gneiss from Ficure 24. Section of gneiss along fault-line in

west side of Sterling lake. The hypersthene is
marked with interrupted striations ; the mag-
netite forms irregular black grains and the
pyrite square ones. The plain white is plagio-

limestone quarry, N. E. of Arden, showing
large fragments of quartz and feldspar (ortho-
clase) in a crushed matrix of the same min-
erals, cemented by limonite and decomposed

clase, containing inclusions of apatite, mag- biotite (?). (Specimen No. 273.)
netite and pyrite. (Specimen No. 346.)

hornblendes in a ground-mass of plagioclase with grains of magnetite. The
grain becomes finer as the width of the dike decreases. The gneiss strikes
N. 20° E., with a vertical dip. The dike nearest the lake is two feet wide
and strikes N. 70° W.; the next one, one foot wide, striking N. 50° W.;
the third, N. 70° W:; the fourth, N. 50° E. and two inches wide; the fifth,
N. 30° W., and four inches wide. The camptonite dike which intersects
the ore-body at the O’Neil mine is an olivine camptonite. The ground-mass
is composed of idiomorphic hornblende and plagioclase, with subordinate
magnetite. There are also phenocrysts of olivine. Scattered through the

rock are cavities filled with calcite which may result from the alterations of

462 Report oF THE STaTeE GEOLOGIST.

the feldspar. Some of the cavities contain feldspar which has altered to
chlorite around the edges, while the centre of the crystal is a mass of
small green epidote grains. Another camptonite with a structure somewhat
resembling diabase, cuts the red gneiss northeast of Long pond near Monroe.

A much sheared dike occurs on the east side of the road, one-half
mile north of the Sterling mine. The section shows a fine-grained ground
inass of a greenish mineral resembling serpentine, and small rods of feldspar,
mostly Karlsbad twins. There are also phenocrysts of a monoclinic feldspar.

f this rock on account of its being so

Little can be said of the relations o
decomposed.
Quartz-Porphyry. A dike of this rock occurs in the Bradley mines.

The hand specimen resembled a fine-grained auartzite, but the section shows
roo) 4 ?

rc

FiGukE 25, Olivine-augite camptonite; showing F1Gure 26. Quartz-porphyry from Bradley mines};

phenocrysts of olivine in a ground-mass of showing phenocrysts of zonal feldspar and a
plagioclase, granular pyroxene and magnetite. granular ground-mass of quartz and feldspar,
(Specimen No. 16.) with shreds of decomposed mica and secondary

limonite. (Specimen No. 354ce.)

a finely granular ground mass of quartz and feldspar, with shreds of decom-
posed mica and secondary limonite. The phenocrysts are monoclinal feldspar
showing a well developed zonal structure, the zones being a granular
decomposition product, probably serpentine. The occurrence of this dike is
unique, surrounded as it is on all sides by the more basic camptonites.
Quartz porphyries have not been hitherto recorded from the Highland

region of Orange county.

Pleistocene Deposits.
The pleistocene formations of the county consist of gravel and sand
deposits, boulders, clays, and lacustrine, as well as alluvial beds. There is a

drift mantle of varying thickness over the rolling country underlaid by the

"LONSNSNW LV YSAIY AWNISYSASN ONOW SLVIS SNdOSJZ SO S3AIND

WIXX sLW1d

Rizrs—Groniocy oF ORANGE County. 463

Hudson river formations. In the valleys this is often of considerable thick-
ness, due to glacial stream accumulations. The valley of the Neversink river
is filled to a considerable depth with gravel, which forms a broad, flat
bottom, and with its covering of loam produces an admirable farming land.
A hole was drilled through the drift at Port Jervis to a depth of 113
feet, without striking bottom. Boulders were abundant in the upper thirty
feet, but below that, the material was mostly quartz sand with an. occa-
sional boulder.* Similar gravel accumulations occur in the valley of
Shawangunk kill along the eastern base of Shawangunk mountain. The
modified drift here partakes of the nature of hillocks, whose summits are all
at about the same level of 900 feet A. T. The intervening depressions are
often occupied by ponds. These hills extend south of Otisville for some
distance, but are there less conspicuous. They also extend around the spur
of the mountain to the southwest of the village.

Around the edge of the Drowned Lands, the gravel rises in rounded
knolls sometimes to a height of eighty feet. There is also a conspicuous
series of kames around Campbell Hall, north of Goshen. Gravel hills also line
the sides of the Wallkill valley.

An interesting train of boulders is to be seen stretching from the
Marlborough mountains across Newburgh and New Windsor townships and
as far south as the Forest-of-Dean iron mines. They are of variable size and
shape and sometimes fossiliferous. West of Newburgh they are sometimes so
thickly strewn over the fields as to make cultivation impossible. M. J. N.
Weed, of Newburgh, who has carefully mapped the limits of this train of
boulders, informs me that he has found these erratics on the slopes and
summit of Snake hill, and farther south in the Highlands at an altitude of
1,200 feet A. T. Two of these boulders are of such large size that it seems
worth while recording the information that Mr. Weed kindly gave me con-
cerning them, because they have been partially destroyed by the improve-
ments made in the city. Mr. Weed writes:

“The ‘Big Rock’ boulder, formerly located in the city of Newburgh, on
the northeast corner of First and Stone streets, was measured in September,
1890, just after the workmen had begun to blast it away. At that time it
measured sixty-two feet from north to south, and eighty-eight feet from east

fo)

to west, and was fourteen feet high. The measurements were made at the
ground but, according to the laborers, fully six feet had already been blasted

off the top. The boulder had a rounded form above ground.

* Report G 6, Pennsylvania Geological Survey.

464 Report OF THE STate GEOLOGIST.

“The second boulder is on Gidney avenue, near the limestone ridge and
cliffs, known as “ Limestone hills,” on the south side of the avenue, and about
200 feet from it. It hes on a gentle east-southeast slope, and the longer axis
lies in a line N. 20° E. The length of the boulder in this direction is
seventy-one feet; breadth at right angles forty-nine feet, nine inches; circum-
ference parallel with the surface at half the height, 188 feet; longitudinal
measurement over the top, from ground to ground, 130 feet; transverse, over
the top, 87 feet.”

Mr. Weed further writes that the sandstone boulders occur in abundance
on Cronomer’s hill, about New Mills in the city, at Stewart’s farm, southeast
of Powder Mills (very large and abundant), and at Vail’s Gate.

Another area of boulders occurs in Tuxedo township, west and south-
west of Southfield. They are all of gneissic rock and occur singly or in
groups. Several large limestone boulders were found on the slopes of
Mounts Adam and Eve. The peculiar manner in which they have weathered
is well shown in the accompanying plate.

The terraces in the valleys are of two classes, estuary terraces and stream
terraces. The stream terraces are best developed in the valley of the
Delaware river. The first terrace above the river and one representing its
flood plain, is 420 feet A. T. The greater part of the villages of Port Jervis
and Matamoras are built on it. There is a second terrace about 475 feet
A. 'T. It forms a broad, level bench on which the upper portion of Port
Jervis is built. It is underlaid by more coarse material than the lower one.
This bench extends up the Neversink valley to a considerable distance.

Along the Hudson river from Roseton to Cornwall-on-Hudson and
around West Point there is a level or very gently sloping quaternary terrace
of variable width. It is mostly underlaid by clay and sand, but sometimes
by boulder till. The clay, which is of great economic importance, was
deposited during a post-glacial depression of the Hudson river valley which
amounted to eighty feet at New York city and 240 feet at Albany. The
terrace at Newburgh extends up to 210 feet, and at West Point it is 180 feet.
At Roseton the terrace is only 120 feet, but it may represent the lower terrace
Which is found at other points along the river. The estuary material at
Roseton is also found at higher altitudes.

South of Newburgh, the terrace broadens rapidly until it reaches its
greatest development around Cornwall. This town as well as Newburgh
and New Windsor are situated on the terrace. At Cornwall, much of

the terrace is underlaid by boulder drift, and an excellent section is

PLATE XXIV

WYNKOOP'HALLENBECK CRAWFORDCO

GRITS OF ESOPUS FORMATION, WITH EASTERLY DIPPING CLEAVAGE, SOUTH OF HUGUENOT.

Rrzrs—Groiocy oF OrANGE County. 465

seen at the north end of the Cornwall station of the West Shore rail-
road. Around the mouths of Moodna river and Quassaic creek, the delta
deposits form a large portion of the terrace escarpment. The southern
portion of Newburgh is built on the delta deposits of Quassaic creek. The
deltas show a characteristic structure and their materials are coarse sand and
gravel, with patches of coarser material in places where the currents were
swifter. They often overlie the clay to a thickness of from ten to fifteen feet.

Good sections of the Moodna delta can be seen from the train as it
crosses the New York, Ontario and Western railroad bridge about one and
one-half miles northwest of Cornwall. The clays underlying the terrace
vary in thickness. At Roseton there are 270 feet of clay under the terrace,
108 feet of which are above river level. The clay is greyish blue and
generally weathers yellow in its upper portions. It is often capped by
several feet of fine sand and gravel. At New Windsor the clay is yellow,
tough, and frequently contains glaciated boulders three to four feet in
diameter. Just north of Cornwall, at Hedge’s brick yard, the clay at the time
of a previous visit by the writer in 1891, showed that peculiar crumpling
of a few layers between undisturbed ones, noticed at other localities and
described in the Tenth Annual Report of the New York State Geologist,
page 189. This distortion is produced, either by a slip, or by pressure of the
overlying delta deposits.

Another terrace area begins north of West Point on the southern slopes
of Crow’s Nest, and continues to a short distance south of the point.
The shore line here is 180 feet A. T., and the government buildings are
situated on the terrace. The underlying material is mostly boulder till,
which is well exposed in the railroad-cut just north of West Point. From
West Point to Fort Montgomery there is little evidence of terrace material,
probably because the low ridge of gneiss along the river prevented the
deposition and facilitated the erosion of much estuary material.

Of importance among the quaternary deposits of Orange county are the
numerous old lake-beds which especially abound in the Hudson river area.
The lakes were formed by the damming up of the valleys and depressions
between the slate ridges, and they disappeared through the subsequent filling
of their basins or the cutting down of their outlets. Black soil underlies the
surface to a depth of from five to fifty feet, and this, according to Mather’, is,
in turn, underlaid by marl. I was not able to find any evidence of this, either

by personal observation or inquiry. The largest of these old lake bottoms is

* Geology of New York, First District, 1842, page 16.

50

466 Report or THE STATE GEOLOGIST.

the Drowned Lands, which until fifty years ago was an undrained and useless
swamp, but is now rich farming land. This area extends from Denton on
the north to the New Jersey state line, a distance of twelve miles. Its width
is from two to three miles and its area within the county, 17,000 acres.
The lake had its origin in a drift dam northeast of Denton. The Wallkill
river follows a winding course along the western side of this area, and sub-
merges it entirely during the spring floods. Other lake bottoms are the
Greycourt meadows, Black meadow swamp, Pine swamp, ete.

Several excellent examples of lake-filling are to be seen in Orange
county. Of these the swamp at the north end of Orange lake west of
Newburgh shows the former extent of the lake. Others are Glenmere lake
east of Florida, Little Cedar pond two miles southeast of Sterling, and Little
Long pond two miles south by east of Southfield. The rocks are often
scratched and smoothed by the ice, and a fine example of glacial polishing
northwest of Monroe deserves special mention. ‘This is in a field west of the
road from Monroe to Bagg’s clove and just before a road turns off to the east
along the base of Bull hill towards Oxford. The Oriskany quartzite has here
been polished until it presents a surface like a mirror, and objects can be
distinctly seen reflected in it. On Shawangunk mountain the striae are
N. 30° E. and N. 60° E.

Economic Geology of Orange County.

Roap Marerrars. Orange county has an abundance of good road-making
materials, but in few sections of the ‘county are they taken advantage of, owing
either to indifference on the part of those persons on whom the maintenance
of the roads depends, or to a lack of the knowledge of the value of these
materials.

The old method of working the roads by digging a mass of loose stones,
dirt and roots from the roadside and throwing it upon the road, is still
followed to a large extent, with the usual poor road resulting. This is the
mode in regions where good material is near by, and even known to the road
repairers. Their use, however, requires a trifle more labor,

The road-metals found within the county are: slate and shale, limestone,
sandstone, granite, and gravel.

Gravel and Sand The gravel has the most extended use of the available
road materials of the county. The localities furnishing it are too numerous to

require mention, and are found in every township. When the gravel is

"3AQ LNNOW NO AduVNO ALINVYD

AXX 431V1d

Mal he

Rizrs—GEOLOGY OF ORANGE County. 467

argillaceous or contains a great admixture of fine sand it makes only a fair
road, but a top-dressing of five or six inches of moderately fine gravel, evenly
laid, generally produces good results. In Tuxedo township very excellent
roads are maintained by using sand and gravel, but this is partly because a few
men are constantly employed going over the roads and repairing any break
that appears. This method costs the township $40 per mile per year, and
there are 2,400 miles of road to be repaired.

Slate. About two-thirds of Orange county is underlaid by slate, and the
roads within this area are usually good where there is not a deep covering of
drift. A layer of siliceous slate produces a smooth, hard road, which in dry
weather makes comparatively little dust. This material is extensively used in
the Neversink valley northeast of Port Jervis, and the roads in that region are
among the best in the county.

A gritty shale or slate causes less mud than an argillaceous one. The red
Longwood shales northeast of Highland Mills make an excellent road-metal
and are extensively used around Central Valley, Highland Mills and Woodbury
Falls. Several large quarries have been opened in this rock on the south-
western slope of Pine hill.

Around Port Jervis the Marcellus and Hamilton shales are also used
with satisfactory results.

Sandstone. The Shawangunk grit makes one of the best road materials
in the county. Its chief use, however, is for railroad ballast, and there is a
large quarry in this rock one mile west of Otisville. This quarry is on the
property of R. Roberts, of Otisville, but it is leased at an annual rental by
the New York, Lake Erie & Western railroad which operates it with a
foree of one hundred men for about five months every year, with a
daily output during that period of about 275 tons a day. The bore-holes
have to be made with hand drills on account of the numerous irregular
cracks which traverse the rock. The stone is broken in a Blake ‘crusher at
the quarry.

Granite. The stripping and trimmings from the granite quarries at
Mounts Adam and Eve are used to some extent for making macadam roads
in Goshen.

Limestone. The Calciferous limestone is quarried southwest of New-
burgh for macadam roads. It is somewhat siliceous and makes a good
paving material after being crushed and screened at the quarry which
belongs to the Miller Brothers. The stone sells for $1.00 per ton, and the

quarry is operated about two months every year.

468 Report oF THE STATE GEOLOGIST.

Gneiss. A mile southeast of Southfield and along the Erie railroad is a
large quarry in the quartzose gneiss. It is operated solely for road-paving
purposes. The rock is crushed and screened at the quarry.

Mr. Josiah Mead is the owner. The material is all shipped to Colfax &
Steele, of Paterson, N. J.

Brick-Ciays. These are the only grades of clay found in the county.
The important and most extensive development of this material is along the
Hudson river, in whose valley there exists the greatest brick manufacturing
industry of the United States. The clay beds extend almost continuously
from Roseton on the north to Cornwall on the south. The firms engaged in
the manufacture of brick in this area together with the location and the

capacity of their brickyards, are enumerated in the following list :

Locality. Workers. Owner. Capacity
in millions.
Roseton, . . . Jova Brick Works, Jova Brick Works, 22
J. Rose & Co., Rose Brick Co., 40
New Windsor, E. Lang, E. Walsh, 8
J. Gillis, J. Gillis, 4
H. Davidson’s Sons, H. Davidson’s Sons, 4
W. Lahey, W. Lahey, 10
David Carson, David Carson, 4

Cornwall,. . .C. A.& A. P. Hedges, C. A. & A. P. Hedges, 10

Goshen,. . . . 1. van Lengen,

bo

The chief market for all, except the last on the list, is New York city
and Brooklyn.

A detailed account of these clay beds has been given by the writer
in the Tenth Annual Report of the New York State Geologist, and only a
general mention of them need be made here. The greatest known thickness
of the Hudson river clay is at Roseton, where there are 108 feet of clay above
the river level and 170 feet below it, as determined by a drive-well, giving a
total thickness of 278 feet. Between Newburgh and Cornwall the clay is
generally tough, with more or less boulders scattered through it, and there is
a varying cover of delta material. The clay at Roseton and Cornwall-on-
Hudson is, on the contrary, well stratified and very soft, but it is likewise
overlaid by delta deposits. The soft mud process of manufacture is the one
used at all the yards, and only common brick is made.

The following is an analysis of the clay used by the Jova Brick Works

and furnished by them :

)

i Mont somaLy
B

MAP OF THE REGION AROUND MONTGOMERY SHOWING THE STRIKES AND DIPS OF THE HUDSON RIVER SLATES WHICH UNDERLIE THIS AREA.

Rirs—Gronocy oF ORANGE County. 469

Din Orr Crease reed. ET 2 | §5.00
Iromeamimemmimas “See Ses ea OS. a 84,54
Lime, Peper naan tens oe IE Re bad
Magienigg 00 = ld ghee Be BEB
AC enero tua Cosme VS Sale 48
Witte me eten nner ne se Ne 8

100.00

The clay deposit at Goshen is local, covering several acres and having
a depth of about thirty feet. The yard is run to supply the local demand.
Drain tile is occasionally made.

The following analysis of clay from the Drowned Lands is given in the
New Jersey Geological Survey’s report, 1891:

SE ata ere m erm cam GeO ee B00
AE ee er ire rene ee nds as. -28,00
ih CoC rece nese Nee ka | LD
Ce rate en ok oe eee SMe 5 Yaw)
NS eae eh Oi an ee, a, s,s 2.60
rm Ute ee a =—-410
Pe a ee ese oh mG os ew ks | OO
"i hse ie DR A Ss 2 a eR 50

100.80

Limz. The limestones of Orange county are all magnesian with the
exception of those of the Helderberg series. While many of the large ledges
in the county have been quarried for lime at one time or another, but little is
made at the present day. There are several kilns in operation two miles
southeast of Monroe, and considerable lime is also being made from the
ambrian limestones west of Newburgh. These are the only two active
localities. ‘There was formerly a very large amount of quarrying done in the
limestone ridge northeast of Arden to supply flux for the furnaces. Another
active quarry was southwest of Otisville, in the Pentamerus limestone.
It is probable that most of the Orange county limestones contain a rather
high percentage of silica.

Leap. Lead occurs in fissure-veins at many points along the Shawan-
gunk mountain, and the prospecting of these caused considerable excitement
in former years. The largest opening made was at Guymard, in Mount Hope
township, eight miles from Port Jervis. The deposit is a true fissure-vein.

470 Report OF THE STATE GEOLOGIST.

It is three to four inches wide and runs N. 70° E. Several shafts were
sunk, and one was carried down 400 feet. The surface rock ts Shawangunk
grit, but the vein no doubt reaches the conglomerate.* Crushers and jigs
were used to concentrate the ore and separate the sphalerite. The mine has
been abandoned for fifteen years.

Buitpine Stone. The most important quarries are in the granite of
Mounts Adam and Eve, and Pochuck mountain, all in Warwick township.

The Adam and Eve quarries are in a coarse-grained granite, but those on
Mount Adam have been little worked on account of the variable character
of the granite which is cut by numerous irregular pegmatite veins. The
Mount Eve quarry, however, is worked by the Mount Eve Granite Co. The
granite of Pochuck mountain is coarse grained and lighter colored than that
of the two preceding quarries. The quarry has been in operation for about
five years. It is situated about one-third the distance up the mountain. The
owner is Mr. Hinchcliffe, of Paterson, N. J. Large dimension blocks are
obtained from this quarry, and most of them are sent to Orange, N. J. The
limestone of Mount Lookout has been used to a limited extent for building
purposes. It has been put in the Presbyterian, Methodist and Roman
Catholic churches at Goshen.+

The Shawangunk grit has been used by the Erie railroad for abutments.

Fracsrones. The Hamilton and Chemung flaggy sandstones have been
utilized to a small extent for paving, the former being obtained from Skunne-
munk mountain in Monroe township, and the latter from the western part of
Deer Park township.

Those on Skunnemunk mountain are the Davidson quarries below the
Seven Springs Mountain house, and farther down the mountain on O. H.
Cooley’s land, northwest of Monroe. The strata are thin-bedded sandstones
of irregular thickness, and are often broken by many joints. Those thus far
opened have been of little value on account of the irregular character of
the rock.

In Deer Park township the stone is of similar nature, but slightly
better. Many openings have been made and a few of these are still operated
at times to supply the local demand. The more important ones are those of
Mr. Myers and the Jackson Bros., west of Rose Point, and Robert Coulter’s,
north of Sparrowbush.

Iron Ores. There are many small and a few large deposits of iron ore

in the Highland region of Orange county, and in former years there were -

* Report G 6, Pennsylvania Geological Survey, p. 161.
+ Bulletin New York State Museum, Vol. IL, No, 10,

PLATE XXVII

o,°9 99
Ooeeeal

. S500 60
Pleistocene oo 6
Chemung =
Zor

Hamilton,including [2224
Marcellus

Onandaga limestone x¥ gS oe
SE SS

OrisKany sandstone as
and Esopus slate oe!
eS

Helder berg limestone : ey,
oe

Medina including

neida

_

=<

(fe °
fp 1
ty °o
/ <
fb ° Oy
(20 (—7
AS , GY |
Goo REP
om ° AH
° Oa
Woo to
ws 0 =
Be o “7
©? r x
Ao fae
j x: Hq
° ra

—
ce
AH

ie
i
IL

Sie ro e i
“Mr:
ae NW AP Lee

i

sz =. ° os

rr

F//N ey verse 5) -
Gi GEOLOGIC MAP OF DEER PARK TOWNSHIP. Scaty 1 1x. — 1 st. WV y)

Rires—-GEoOLoGY OF ORANGE Counry. 471

many active mines. The majority of these are no longer in operation, owing
to the poor quality of the ore and the cost of operating them. In many
instances the ore had to be hauled three or four miles. The two active
mines are the Forest-of-Dean, in Woodbury township, and the mines of the
Sterling Iron and Railway Company in Tuxedo township, at the southern
end of Sterling lake. The Sterling mines were in operation during the
Revolutionary war and have so continued since. Many openings have been
made in the area around the lake, and abandoned after being worked to
various depths. The company owns 20,000 acres of land and the following
mines are on it; Crawford, Behring, Moorhead, California, Sterling, Clark,
Lake, Oregon, Spruce Swamp, Hard, Cook, Scott, Mountain, Causeway, Long
and Augusta. The oldest and most important is the Sterling mine which
was opened in 1750, and a furnace built in 1751. The ore-body is of large
size and, according to Smock*, has undulating foot-walls, the rolls running
N. E.and 8. W. There is said to be a fault on the south side of the mine
by which the ore is displaced ten feet. At present the slope of the Sterling
mine has gone down 1000 feet on the dip. Levels are run off every fifty
feet (see figure) and after all the levels are driven, lifts will be sunk
between them. The thickness of the bed varies from five to twelve feet
and the ore is sharply defined from the walls.

The Lake mine lies to the north of the Sterling and evidently is a
portion of the same ore-bed which has been divided by a pinch. This pinch,
is about 250 feet long. The slope of the Lake mine, which descends
diagonally on the dip, is 1100 feet long and the ore-body extends under the
lake. The wallrock of these two mines is a hornblendic gneiss; associated
with the magnetite along the border of the ore-body are amphibole, pyroxene,
epidote, red and white feldspar, tourmaline and quartz. Beautiful inter-
growths of quartz and tourmaline are common.

The Sterling ore averages sixty per cent. iron and four per cent. phos-
phorus; the Lake mine, fifty-nine per cent. iron and nine per cent. phosphorus,
while the monthly output of the two mines is respectively 4000 tons and
2000 tons.

Compressed air is used to operate the drills and one of the compressors
is run by water-power derived from Sterling lake. Plate XLII shows the
surface workings of the mines, the dump-heaps seen up the hill being from
the quarry workings of some of the abandoned ones, for the ore-body of the
Lake and Sterling mines formerly extended up the surface of the hill, there

* The Iron Ores of New York.—Bulletin New York State Museum, Vol. IL , Number 7.

472 Report oF THE Stare GEOLOGIST.

being little or no rock covering the ore. The old Clark working is half-way
up the hill, and affords a fine example of pinching and swelling of the ore-bed,
as shown in a foregoing figure. Considerable ore has been obtained from
this mine.

One mile to the northeast of the Sterling mine, is the Augusta mine,
which was of considerable importance in former years. A plan of the
ore-body is shown in Plate XLIX. The ore had been mined for a distance
of 100 feet on the dip. This mine has been recently opened again. A
longitudinal section, or rather side elevation of the section, is given in the
lower portion of the same plate, and in Plate L are shown a number of
transverse sections drawn along the lettered lines indicated in the upper
drawing of the previous plate. It will be seen from these that the ore-body
was long and flat. A fine fault is exposed in the hanging wall at the mouth
of the mine (Plate XL). The exact amount of displacement is not known
and it does not show in the sections of the ore-body.

The Causeway and Mountain mines include several small and parallel ore-
bodies, which are shown in plan in the upper portion of Plate L. <A side
elevation of the section of those of the Mountain mine is also shown in the
upper right-hand portion of the same plate. It will be seen from this that in
each case the ore cropped out at the surface, and that in one instance the
bottom of the ore-body had not been reached when the mine was shut down.
The writer is indebted to Mr. Knox, the superintendent of the Sterling mines,
for permission to reproduce these sections and also for other information
concerning the mines in this region.

The Scott mine is a mile and one-half northeast of the Sterling, and was
formerly of considerable importance. According to Smock*, it has reached a
depth of 430 feet on the slope and its levels have an extreme length, along the
strike, of 900 feet. The ore-bed is four to eighteen feet thick. At the Cooke
mine, which is south of the Scott, the shaft has a vertical depth of 250 feet.
None of these mines afford bessemer ores.

The Forest-of-Dean mine is situated five miles west of Fort Montgomery.
It has been inactive for a considerable period, but was started up again
last August. The mine is owned by the Port Henry Iron Co. and is
operated by the Forest-of-Dean Iron Co. The ore-body is large and some-
what lenticular, with a thickness of ten to forty feet, and a width of as much
as eighty feet in places. A slope is sunk on the pitch which is 22° N. E. and
the full width of the vein is stoped out. Pillars are left at intervals to

3 Loc. cit.

Mii MY Ml .
Y YY Wf Hy, Y PSL We Gx,
Wy W yy Ij) ff
<p JV) y

Cambrian limestone

Rirs—Gronocy oF Oranck County. 473

support the hanging wall. The wall-rock is a feldspathic biotite gneiss which
dips steeply to the east. The ore-body is cut by a camptonite dike six feet
wide, and a horse divides the ore at the roof, but farther down extends across
the ore-body. According to Smock, this horse shows a synclinal structure,
Figure 21 gives a section and plan of the ore-body.
The ore is non-bessemer and the following analysis of it is given in

Smock’s report :

isco tee ss 8.80

UN UE coe? ee CU, sg cg ete ee | tac

Lime, Per may stat tn LOL

JUST GST 2,7 GN Se Ue ee Se nee ee a)

Peete ea aGr MEAD Sue et ste tse ee see be 63

eect OmUNOle i. ayes eet olive wel ees os, «| 83.56

Pe OMM ORM ener Nese tet le ee ss) ese, , “280
OAT yOnnG Ate Go toes eee gs SOU ae Ak re en am O05
Ce Serie ONT st ela eee cee gs 20

99.44

The slope is about 1,600 feet long, and the ore is raised in a car. It is
trammed to a point within two miles of Fort Montgomery, whence it 1s carted
tothe river. ‘This item of transportation would greatly increase the cost of
operation of the mine were it not for the fact that the entire plant is operated
by water-power. This is generated by two overshot wheels forty feet in
diameter and six feet wide. The mine-water is raised through a vertical shaft
located 900 feet east of the mouth of the slope. The ore is used in the
furnaces at Poughkeepsie.

Soms. About two-thirds of the county is underlaid by the Hudson
river slates, which are usually thinly covered with drift. The soil of
this region produces excellent hay and the area is extensively given over to
dairy farming, the products of which have made the county well known.
Very little else is raised in the slate region, except in the northeastern
portion, where the stony soil and hilly ground produced by the coarse drift
and sandstone, are admirably suited for the cultivation of grapes.

The limestone areas afford a good soil, in their more elevated portions,
but they are often areas of depression and occupied by swamp land.

These swamps, however, occur not only in the limestone region, but also
in many parts of the slate area and form perhaps the most important agricul-
tural feature of the county. The rich black soil of the swampy tracts is

474 Report OF THE STATE GEOLOGIST.

enormously productive, and some of it is worth $300 an acre. This soil is
generally planted with onions, and 700 bushels per acre is not an uncommon
yield. Potatoes or corn are generally planted in alternate years to relieve
the soil. There are about 40,000 acres of swamp land in Orange county. The
largest of these areas is the Drowned Lands in Warwick, Greenville, Minni
sink, Wawayanda and Goshen townships and covers 17,000 acres. Until
about sixty years ago the area was covered by several feet of water held
in by a natural dam of glacial drift at the north end. A canal cut through
this dam has redeemed the land. From the Drowned Lands there arise islands
of limestone or drift, which are named Pine, Great, Pellet’s, Gardner’s,
Merritt’s, Cranberry, Black Walnut, Fox and Seward islands. Other import-
ant Swamp areas are: Greycourt meadows, covering 500 acres and extending
from Craigsville to Chester; Black meadow in Goshen township, 1,000 acres ;
Long swamp, southwest of Edenville in Warwick township, 1,000 acres ;
Tamarack and Purgatory swamp in Hamptonburgh; Big swamp, north of
Orange lake; Great swamp, near Coldenham, New Windsor township; Great
Pine swamp, which begins near Howells and extends northward and east-
ward about seven miles in the town of Wallkill; Little Pine swamp, east of
Thompson’s ridge; Pine Bush swamp in Crawford township, Pakadasink
swamp in Greenville, and Barton swamp in Cornwall township.

Mrverat Sprives. The only mineral spring in the county, of which
the writer has any knowledge, is a chalybeate one, in the Highlands east of
Mountainville. It is known as Sutherland’s spring.

Warrer Power. Aside from the small streams furnishing local grist
mills, water power is supplied by the Shawangunk kill, Wallkill river,
Moodna creek, Quassaic creek and Ramapo river.

The Shawangunk kill is little used, except for small grist mills. The
Wallkill river is a sluggish stream with little fall until it reaches Walden and
Montgomery, at both of which points it cuts down through the Hudson river
slates. Two mills and a paper factory are in operation at Montgomery where
the fall is mereased by a dam across the river.

At Walden the river has a natural fall of twenty-six feet, but since the
dam above the bridge was constructed, a fall of thirty-two feet is obtained.
This fall is utilized by the New York Knife Co., employing 350 hands. The
water passes though six turbine wheels, which generate 195 horse-power.

Mr. Moore, the superintendent, estimates that, even in dry weather, there
is sufficient flow of water to furnish 1,200 horse-power. The reclaiming of the

swamp lands farther south has had a material effect on the stream. The

B3Lv1S Y¥3SAIY NOSGNH SO $395037 HLIM 'NA3G1WM Lv YSAIY WUATIWAA

al Pr MOSSNSTIVHOONNAM

XIXX S3LV1d

Rirs—Gerotogy oF ORANGE County. 475

Wallkill Valley Knife Works, below the bridge, receive sixty horse-power from
the river. Orange lake supplies Quassaic creek which flows southeast and enters
the Hudson river at the south end of the city of Newburgh. The flow of
water from the lake is regulated by gates, but there are so many firms receiving
power from the stream that in a dry season, like that of 1895, they have to rely
wholly or in part on steam-power. Between Orange lake and the powder
mills there are several small grist mills receiving power from the creek. In
spring and early summer the creek is utilized by the powder mills.

Within the city limits the factories receiving water-power from Quassaic
creek are :

. Newburgh Woollen Mills, twelve feet fall and one wheel furnishing
twenty-eight horse-power. ‘This is used from February to May, depending on
the season.

Saxony Silk Co., eighteen feet fall, two turbine wheels, thirty and forty
inches respectively, which together furnish seventy horse-power. They are
used about seven months of the year.

Ross’s flour mill, twenty-four feet fall, sixty horse-power. Used nine
months of the year.

Newburgh Bleachery, twenty-one feet fall, and one hundred horse-power
derived. Used eight months of the year. This factory has a large reservoir.

~ Adams & Bishop Paper Mill, Little Falls Paper Co., and Hudson River
Woollen Mill. These three all receive a small amount of power from the stream.

Moodna creek is utilized at Salisbury Mills, but otherwise is of no
special importance.

The Ramapo river furnishes power to several grist mills at Monroe and
one at Turners. Its branch entering at Arden is an active stream with
considerable fall and could no doubt be profitably utilized.

The Neversink river is not utilized for water-power and has little fall
within the limits of Orange county.

Warer Suppry. <A word should be said regarding the water supply of
the towns within this county. There is a large number of lakes, especially in
the Highland region which contain an abundant supply of clear water. Of
these Long pond, south of Monroe, supplies the town of Chester, and a pipe is
being laid from Mount Basha lake to supply the town of Monroe, two miles
north of it. Little Long pond in Highland township, furnishes the Government _
reservation at West Point, while Little pond west of Newburgh furnishes that
city with its drinking water. The city of Middletown has constructed a
reservoir by damming the valley of a creek to the northwest of the town.

PLATE XXX

¥ » mrs a i ne Aus rag ee,
< e ER a si
ey

Yypy jie re =) /
eas ap ! :

VE
ie

Dy ee
caeee

NM, yy je ;
M/ Y YX =), Se
Uy | q is SN indsor
W// NK) Y Y

7 x . oy eae La Hi
UY TINS as

ig
Ks

We Ly We Ye Li

Cambrian ener) en Fits i
egnelss

Seige

GEOLOGIC MAP OF NEWBURGH AND NEW WINDSOR TOWNSHIPS, Scaue 1 IN, = 2 MI.

AY

\\

* a\\

quer oe Fgaod BAUNERWOT MORTAR wand
. (Sea tia ae
i i ; ae wee

‘ a}
, he
=
: ~
}

-
1 aaa 4

“ f

i za
eg ge Li
»
hay :
i

“HOYNEMAN JO HLNOS GVO Y3SAIN ONOIV SNOLSSWIT NOLNSYL

IXXX SLW1d

oe
aan *

HS

inl
Tf,

>
a/

SNIW NOU! TIANO

‘OD GHOIMVHO NOSANSTIVH dOOWN

(IX XX JLW1d

‘ONITYSLS YVAN ‘SNIW VISNONY 3O T1VM SNISNVH NI LINv4

IIXXX dLV1d

‘"QNV7 SHL SO GNSS YSHLYVS SHL LY 3YV SANIIN NOY! SHL ‘HLNOS ONIMOOT ‘Sy¥v1 ONINYSLS

=~

=~
° DIFYOAMVYD ROIGNATIVH YOON. M4

AIXXX 31LVW1d

‘ANIW TIANO LY AGOS-3YO ONILLND 3yIq

Pray,

+ gen os?

AxXX 3LW1d

‘HLNOS DNIMOOT ‘A¥V1 GOOMNASYS JO M3IA WasaNa5

IAXXX S1V1d

‘09 QHOAMVYO MOSENATIVH dOOMNAM

PLATE XXXVI

TUXEDO LAKE, LOOKING NORTH.

‘STMANSO YV3SN Y301NOS SNOLSAWIT

IIAXXX SLW1d

"LNIOd LSS WO8S HLYON ONIMOOT 'SGNYIHDIH SHL SO M3I/A

XIXXX S1V1d

yf) Ore
ae ut ey

*

PLATE XL

+Coldenhom

~
‘:
~
«Mrdys van

\Crawford Jen

Iron Mines
Lead Mines
Clay-banks
Lime-stone Quarries
Granite Quarries
ondatone Quarries r?
4 ak lle

cadmetal Quorries

p |
4 \
: Me

MAP OF ORANGE COUNTY, ILLUSTRATING ITS ECONOMIC GEOLOGY,

PLATE XLI

"y Wer ints

!
uarr

-

Sur face.

y

a
i

ee
a al ,
1 ary

t
(om

x

Le

PLATE XLII

ooo Battom of mine, huathoat bate of ey

103.5"
10%.
NS.3"
(286°

~ . rs ’
° a7
tf

a,
1-17 = 662"

Vertiecl sectvon representing outline of eredodces shown en plan below. |

st Rodi
any!

Detail of Workings AB

Ep LG: Scale /*~ 30'
a *

(GEES

— aca
Wie ee a
SSE F ia

See: ESTES ae S

nie

Seotibes through Ore-body ol Augusta Thine.

The sections are along franverse broken lines
Shown in the preceding plate.
=~

AS ae es aS ae Sere
emma “sacl

Ca ee S) tee
_————— rs
oe

| i a
Fe te aS

ee
ee:
a |
ret
baa

“F

>. my
-

i

7

a?

‘air
t
2

-
a’ es
s
» !
, i
‘
et I
Fd
~
Ps

GEOLOGICAL SURVEY-OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

REPORT
ON THE CRYSTALLINE ROCKS OF ST. LAWRENCE COUNTY.

JAMES HALL, | Cae Shy PES diz.

State Geologist. Assistant.

1895.

J sh Haun, State Geologist.
| ‘Sir :—Herewith I submit a report on the crystalline rocks of St.
_ Lawrence county.
Respectfully yours,
Cr ONO. or:

~ Hamivron Conecr, Crinton, N. Y., Jan. 1, 1896.
479

Report on the Crystalline Rocks of St. Lawrence County.

By C. H. Smyru, Jr.

The field work done in St. Lawrence county during the summer of 1895,
consisted in a continuation of the reconnaissance of the crystalline rocks of
the region, begun some time since, and carried on in part privately, and in
part under the direction of the State Geologist. This reconnaissance has now
been extended over about two-thirds of the crystalline area of St. Lawrence
county, and also considerable tracts in Jefferson and Lewis counties, the total
area covered approximating 2,000 square miles.

The present report is particularly concerned with results obtained in a
new territory comprising the towns of De Peyster, De Kalb, Hermon,
Edwards, Canton, Russell, Potsdam, Pierrepont and Parishville; together
with points re-examined in the towns of Gouverneur, Rossie and Fowler,
which were covered in the examination made during 1893. Certain facts
observed during 1894, in the towns of Pitcairn, Fine, Clifton, and Diana,
Lewis county, which have been already described in part,* may prove of
value in this connection.

In making this reconnaissance, the main object was to learn the distribu-
tion of the crystalline limestone formation, for which the name Osweyatchie
series was suggested in a previous report.f A special effort was also made
to ascertain as many facts as possible bearing upon the question of the origin
of the great areas of gneisses, and the relation existing between these rocks
and the limestones.

Distribution of Crystalline Limestones. As a wider territory was covered,
the distribution of limestones was found to conform to the same order as in the
case of the more limited areas previously described. They form belts, many
square miles in extent, stretching in a northeast and southwest direction ;
and, in addition to these, small scattered patches, irregularly distributed, and
varying greatly in size. By far the largest limestone belt is that which is
traversed longitudinally by the Rome, Watertown & Ogdensburg railroad
from Antwerp to a pomt some two miles east of De Kalb junction. The belt

begins at the former village, but extends some miles northeast of the latter,

* Bulletin Geological Society of America, VI , pp. 263-284.
+ Report of State Geologist for 1893, pp. 493-515.
8 ] 481

482 Reporr oF THE Stare GEOLOGIST.

the railroad leaving it at the point stated. Scarcity of outerops prevents a
precise location of the limit in this direction, but it is probably cut off by
gneiss about two miles south of Canton village. It may possibly, however,
be connected with an area of limestone in the southwest corner of Potsdam,
although the latter appears to be entirely surrounded by gneiss.

The linear extent of this belt from Antwerp to its probable end in
Canton, is about thirty-five miles. Its width in a northwest-southeast
direction is extremely variable. Beginning in Antwerp with an average
width of about two miles, it expands rather suddenly to six or eight miles in
Gouverneur, narrowing again as it passes out of this township to the north-
east. Along the northern boundary of Gouverneur, gneiss appears im long,
harrow strips, whose precise extent 1s uncertain; so that it is not clear
whether or not the Gouverneur limestone belt is separated entirely from a
large area which extends from Theresa, across Rossie and Macomb, and
disappears under the Potsdam, in De Peyster. If distinct, these two belts can
have only a very narrow strip of gneiss between them to the west, and the
indications are that this disappears entirely in the vicinity of Yellow lake, in
Rossie. Eastward, in De Peyster and De Kalb, a large area of gneiss comes
in between the two limestone belts. The southern edge of the Gouverneur
belt is more clearly defined, and an extensive area of gneiss separates it
from the next belt to the south. The latter, which may be called the
Edwards belt, begins in Fowler, crosses Edwards, and seems to run out in the
western part of Russell. Its area is much less than that of the Gouverneur
belt, but it is of economic importance on account of its tale deposits. This
belt is quite sharply defined, although along its southern edge there is a
rather confused mingling of limestone and gneiss, of much interest and
deserving careful investigation. Another wide stretch of gneiss separates the
Edwards belt from the Diana belt, which crosses the towns of Diana and Pitcairn
with a width of about two miles. Directly southeast of this belt, that is,
normal to the trend of the belts, the country has been examimed for only a
few miles, but to the south it has been traversed some thirty miles or more
without the finding of any limestone. However, it is not certain that other
belts may not exist in the forested region to the southeast, although facts to
be stated below indicate that this is probably not the case.

These four belts, or, if the Macomb and Gouverneur belts be considered
one, three belts, comprise a large proportion of the crystalline limestone of
the region examined, The remainder is found in the scattered patches to

Which reference has been made. These occur both near, and at considerable

Smytu—CrystaLuingE Rocks or St. LAwRENcE County. 4838

distance from, the large belts, and range from less than a mile to several
square miles in area. There is nothing to distinguish them from the larger
belts except their limited dimensions, and they must be regarded as
constituting a portion of the limestone series.

As to the character of the limestone in the various areas, it is scarcely
necessary to speak here, descriptions having already been given in the papers
above cited.* It is always highly crystalline, ranges in color from white to
dark bluish grey, and often contains disseminated and aggregated silicates.
Of these, the most important are serpentine, forming ophicalcite, and
tremolite. The latter renders the rock more resistant to weathering, and
sometimes is so abundant as to constitute a tremolite schist. The limestone
contains a variety of gneissoid rocks, some of which are doubtless interbedded,
while others are probably altered intrusives. ‘These gneisses often show
a great amount of contortion and crushing, as a result of the application of
intense pressure. The limestone itself, on the other hand, presents a massive
undisturbed appearance, with no indication of its subjection to pressure
beyond the development of polysynthetic twinning—$R. Owing to the
difference in the nature of the rocks they have been affected very differently
by pressure, the gneiss having yielded by folding and fracture, the limestone
by flow. It is quite possible, however, that a considerable amount of
fracturing actually occurred in the limestone, but this has been obliterated by
subsequent recrystallization.

In considering the small patches of limestone, a point which should not
be overlooked is that, owing to the easy weathering of the rock, outcrops are
more generally wanting than in the case of the surrounding resistant gneiss.
For this reason, the real extent of these areas is probably often greater than
it appears, while there are, doubtless, many such patches that have been
entirely overlooked.

When the distribution of the limestones is viewed in a broad way, it
becomes apparent that these rocks have their greatest development in the north-
western part of the region, decreasing as the eastern and southern parts of the
county are approached. In the former district lie all of the extensive belts,
while in the latter only scattered patches of limestone occur, gneiss being the
prevailing rock. This relation is very marked and is probably persistent
throughout this portion of the Adirondack region. There can be little doubt

that the combined Macomb and Gouverneur belts constitute the most extensive

484 Reporr oF THE Strate GEOLOGIST.

southeastward into the heart of the region. Nevertheless, no fixed limit has
been found in this section beyond which the limestone can be said not to
extend. It does not disappear, but simply decreases, occurring in smaller and
more scattered areas. If it were regarded as a distinct formation (a point to
be considered later), it could not be mapped as constituting a clearly defined
and continuous area, but would necessarily be represented in detached
portions ; and facts now at hand indicate that such portions occur scattered
all through the Adirondacks. Hence the distribution of the limestone forma-
tion is, in a sense, co-extensive with that of the entire series of crystalline rocks
comprised in the Adirondack region; and the task of mapping the limestone
formation, be it called Huronian, as has been suggested, or, as preferred by the
writer, by the local term Oswegatchie, involves the entire problem of the
Adirondack geology. For to map the limestone formation, its geologic
limits must be first ascertained, and this necessitates the determination of
its relations to the associated rocks. In the case of the anorthosites and
gabbros, this has been done, as well as for some minor developments
of granite, etc. But the origin of the gneisses which cover the greater
part of the western Adirondack region, and their relation to the lime-
stone are, as yet, unsettled, and constitute a problem requiring careful study
for its solution. If, from such study, it should appear that the lime-
stones and gneisses together constitute a single series, it would make up
the whole of the area comprised within this report, except where
certain intrusive rocks occur, and would, indeed, with this latter exception,
probably make up the entire Adirondack region. On the other hand, should
the limestone and gneiss prove to belong to entirely distinct formations, it
would be a simple matter to trace their boundaries. But, finally, should it be
learned that some portions of the gneiss belong with the limestone in one
formation, while other portions belonged in another formation, then, judging
from experience in the field, it would become a very difficult matter to trace
the boundaries of the formations, on account of the perfect gradations
generally shown between different varieties of gneiss. The foregoing points
were, in part, touched upon in a previous report, but 1t seems worth while to
refer to them here, bearing, as they do, upon the whole question of aims,
methods and results of geologic investigation in the Adirondack region. One
fact may be safely premised, namely, that the different crystalline rocks of the
region are so related to one another that the study of one involves, to a greater
or less extent, the study of all, and the history of one portion can not be clearly

stated without reference to other portions. This is, of course, meant to apply

Smytu—CrysTALLinE Rocks or St. LAWRENCE County. 485

to the broader problems, and of these, one is certainly the distribution of the
limestones and their relation to the other rocks.

The mere facts of distribution have been given above, their bearing upon
the question of relation to other rocks will be considered in dealing with the
relations of the limestones to the gneisses. This question requires, however,
for its discussion, a previous consideration of the probable origin of the
oneisses,

Origin of the Gneisses. From the foregoing it is evident that the
eneisses afford the chief problem of the region. This problem is twofold,
involving both the origin of the gneisses and their relation to the limestones.
While these two questions are intimately connected, and facts bearing on one
are often equally important in their relation to the other, it may be more
convenient to consider them separately.

In the outset it should be stated that neither question is regarded as
finally settled. It is often very difficult to procure data which bear definitely
upon these questions, and as the rocks involved cover a great area, it is
dangerous to generalize upon a basis of facts gathered in a small portion of
the area. This difficulty has been somewhat reduced by the agreement of
phenomena occurring at widely separated points, but it is, nevertheless, a real
difficulty. In many cases, perhaps in most, no direct evidence is at hand, and
it is necessary to reach conclusions by analogy. For these reasons, particu-
larly on account of the limited amount of study as compared with the
extent of the region, it is not deemed wise to state any very broad final
conclusions, but merely to present such facts as seem to be of importance
in their bearing upon the major problems of the region. What this bearing
is, and to what conclusions the facts in hand seem to lead, must, of course,
be stated; but the endeavor will be made neither to exaggerate the
importance of the data, nor to deal with them dogmatically.

Without going into the history of opinion on the subject, it may be
stated that the gneisses have generally been regarded as metamorphosed

¢

sediments, such parallel structures as they possess being considered as result-
ing from original bedding.

The term gneiss is here used in a very broad sense, embracing rocks
having a wide variation in structure and composition. The chief value of the
term, when used without any qualifying word, lies in its breadth, and this
value largely disappears if the term is restricted to a rock having the compo-
sition of granite. Such a broad term is essential in the present discussion,

not only on account of the lack of detailed investigation, but chiefly because

486 Report oF THE Stare GEOLOGIST.

the different varieties of rock included under it, so constantly shade into
each other, or are so intimately associated as to render their precise differen-
tiation difficult or impossible.

In composition, the rocks range from acidic, like granite, to basic, like
gabbro. In structure they range from fine to very coarse, and from distinctly
gneissoid, or even schistose, to entirely massive. The prevailing type, in the
region here covered, is a fairly acid, light-colored rock, of medium or fine
grain, and rather obscure foliation. It often looks as though its fine grain
had resulted from a crushing of larger constituents. Other important
varieties are: a coarse augen-gneiss and a porphyritic gneiss often extremely
coarse, and nearly or quite massive. The dark-colored basic varieties seem to
be much more limited in extent, the only large area noted being in South
Russell. Brief accounts of some of these varieties have been given elsewhere,
and need not be repeated, as such details as are necessary will be brought out
in discussing the origin of the rocks.

When this latter question is considered, three possible explanations
present themselves as being worthy of careful consideration. According to
one of these, the gneisses are metamorphosed sediments; according to the
second they are of ingneous origin; while the third comprises both of the
others, regarding the gneisses as in part sedimentary and in part igneous.

Dealing with the internal evidence alone, the parallel structures of the
gneiss afford the only support for the hypothesis of metamorphosed sediments.
And when the evidence is examined it appears very weak, for, as a rule, there
is only a foliation which could not be regarded as in any way connected with
original bedding, but is clearly a secondary structure, and often very incon-
spicuous. Distinct banding that might represent original stratification is rare,
and such bands as do occur are generally widely scattered and of limited
extent, demanding, as shown below, a different explanation. Indeed, rather
than showing pronounced banding, the rocks are very uniform in texture and
composition over wide areas, and where they change, do so gradually. It
may be safely stated that there is nothing in the structure of the gneiss as a
whole, which demands, or even suggests, that it should be regarded as derived
from a sedimentary formation. On the contrary, the complete absence of
clastic structure, the lack of any trace of stratification, and the uniformity over
wide areas are all opposed to such a view.

The chief support for this hypothesis is found in the limestone associated
with the gneiss. This is doubtless a metamorphosed sedimentary rock and its

presence in long belts, whose trend is parallel to the foliation of the gneiss,

Smyru—CrystaLLInE Rocks or St. LAwRENcE County. 487

suggests that they may be parts of one great series. This idea is strengthened
by the fact that on the borders of the gneissic areas, as the limestone is
approached, the gneiss is often finely laminated and quite similar to narrow
bands of gneiss which seem to be interbedded with the limestone. But these
laminated gneisses between the massive gneiss and limestone have been found
to be the exception, not the rule, as was formerly thought, and hence, are of
little importance in this connection. As to the parallelism of the foliation
of the gneiss with the strike of the limestone, it is a necessary result if the
foliation is a secondary structure resulting from the same pressure that folded
the limestone.

The alternation of broad belts of limestone and of gneiss, In the north-
western portion of the region, is suggestive of a sedimentary series, in spite of
some peculiarities of distribution, difficult to explaim; but the scattered
patches of limestone occurring in wide areas of gneiss to the south and east,
are difficult to harmonize with this view. It has been thought probable that
the limestone was confined to the region of the extended belts, and that the
associated gneiss might be distinct from that of the southern and eastern parts
of the county. But, as shown above, the limestone has no such limitation,
and there is nothing to distinguish the gneisses of the northern townships
from those of the southern. They must be considered together, at least for
the present, as one great formation, with the limitations and conditions cited
below. It seems clear that if the gneisses of the northern towns belong to the
limestone series, those of the southern towns do as well. On the other hand,
if the latter do not, neither do the former. The reasons, so far as the relations
of the two are concerned, for regarding the gneisses as part of the limestone
series having been stated, it must be admitted that they are extremely inade-
quate. On the other hand, the gneisses themselves, with the exception of
limited areas, lack every characteristic of a sedimentary series. Thus, both
lines of evidence fail almost completely to establish the sedimentary origin of
the gneisses. Nevertheless, the mere absence of proof that they are
sedimentary cannot be taken as proving that they have not this origin. For
it is entirely possible that the absence of proof results from extreme. meta-
morphism, and the evidence sought for might be found at any time, provided
that some other origin can not be established. This latter condition leads to
the consideration of the second hypothesis named above: that of derivation of
the gneisses from igneous rocks,

Taking up first, as before, the internal evidence bearing upon the

question, there are certain characteristics of the gneisses that are of import-

488 Reporr oF THE STatE GEOLOGIST.

ance. They form wide areas between belts of sedimentary rocks, but
themselves, as above stated, showing no trace of sedimentary origin. On the
contrary, they show the uniformity of character that might be looked for in
plutonic rocks, together with the gradual variation so common in rocks of this
class... Such parallel structures as appear in the gneisses have been shown to
have nothing in common with the bedding of a sedimentary series, while they
are precisely such structures as appear in plutonic rocks as a result of
pressure, or of flow before solidification.

Sections of the widespread, fine, light-colored gneiss show it to consist of
orthoclase, plagioclase, and quartz, with mica, hornblende or pyroxene. Either
feldspar may predominate, and microperthite is nearly always present. As a
rule, the ferro-magnesian minerals are in small amounts. With the exception of
the quartz, the constituents are in grains, which often appear to have resulted
from the granulation of larger grains, that is, the structure is cataclastic and
the original rock must have been a coarse, holocrystalline aggregate, such as is
typically afforded in the class of plutonics. Such a rock under pressure

gneisses, and at many points the latter pass by insensible

would yield the g

gradation into such a rock. That they have been derived from it by pressure
is clearly indicated. In some cases this massive core is a coarse, evenly
granular aggregate, in others it is more or less distinctly porphyritic. The
latter 1s perhaps the most common type, forming considerable and widely
distributed areas. The case is analogous to that of certain gneisses of
Canada, in which, as shown by Adams,* the cataclastic structure is usually
accompanied by other indications of an igneous origin; while, in the same
region, gneisses lacking this structure are thought to be derived from
sediments. The fact that a gneiss is formed by crushing of a coarse
holocrystalline aggregate does not prove its igneous origin, as this aggregate
may have been formed by crystallization of sediment. But in the absence
of distinct proof of the latter supposition, the probabilities favor the former ;
and if all other kinds of evidence lead in the same direction, the cataclastic
structure may be regarded as an important indication of igneous origin.

The role of the quartz in the gneisses requires some special consideration,
being, as above indicated, somewhat exceptional. Quite often the mineral
shows the effect of crushing less than do the other constituents. While they
are in small rounded grains, the quartz is often in large masses or long spindles.
As the quartz could hardly flow while the feldspar fractured, the conclusion

is obvious, and seems to be well grounded, that, in the case of the quartz, there

* American Journal of Science ; (IIL) L., pp. 58 to 69.

Smyru—CrystaLtuinE Rocks or Str. LAwrence County. 489

has been crystallization after the production of cataclastic structure in the
rock. While in many cases the quartz was probably an original constituent
and has recrystallized; in others, it is doubtless secondary, the gneiss being
more acid than the parent rock. The microscopic details upon which these
conclusions are based need not be stated here.

Where the cataclastic structure is lacking, the gneisses have the holo-
crystalline granular structure of plutonic rocks, the grain) varying con-
siderably, and, in the coarse varieties, porphyritic structure being particularly
common. Rapid variations of grain are often shown by the coarse porphy-
ritic varieties, fine phases coming in quite irregularly, forming bands and
masses with the aspect of the common, fine gneiss. They lack, however,
the crushed aspect, and appear to be primary variations. The micro-
scopic study necessary to determine this point has not yet been under-
taken. The same localities often show the passage from the massive
into the finely laminated crushed gneisses, the transition sometimes
occurring within a few feet. It often happens that the passage from a
coarse, massive, to a fine, well laminated gneiss is attended by a darkening
of the color.

But in other cases, where the coarse, light-colored gneiss occurs with a
fine dark-colored variety, there is good reason for believing that a different
relation exists between the two. In instances of the latter kind, the fine gneiss
is usually cut by abundant granitic veins, which wander irregularly through
the rock, with a tendency to follow the foliation if it is at all marked. At the
same time, the acid gneiss contains masses of dark rock of great variety
of form and size, and, in every respect like inclusions in an igneous rock.
That such they really are scarcely admits of a doubt, and all uncertainty is
removed where, as has happened in several instances, an irruptive contact is
found between the light and the dark gneiss. Such phenomena point to two
conclusions: first, all parts of the gneiss are not of the same age; and
secondly, the massive, porphyritic gneisses are certainly in part, probably
entirely, of igneous origin, being younger than, and intrusive in the fine, dark,
eneisses. These facts, however, shed no light upon the origin of the latter
variety.

The inference above drawn, as to the true nature of the porphyritic
eneisses, becomes important in its bearing upon the general question in hand,
when it is remembered that these rocks themselves make up a not inconsider-
able part of the gneissic areas, and, moreover, that much of the finer gneiss

is probably derived from them.

490 Reporr or tHe Srare GEonoaist.

As regards these finer gneisses, there is a series of facts analogous to
those described in the coarser rocks, so far as the inclusions are concerned.
At many widely separated points, the fine pink and grey gneisses have been
found to contain masses of very dark, rather fine rock. As it seemed probable
that these masses might have some bearing on the problem in hand they were
examined with care, and in many cases were sketched, or photographed. —They
may, for convenience of discussion, be divided into two groups: long narrow
bands, and irregular masses.

The bands vary in width from a few inches up to two feet or more, and
may be some rods in length. They are seldom, however, continuous for any
such distance, being divided into segments, evidently at one time continuous
but now separated by masses of gneiss, from a fraction of an inch to several
feet in width. To form these segments the bands have been broken squarely
across, so that the blocks have a nearly rectangular or a rhomboidal outline.
The dark rock of the bands is usually imperfectly gneissoid, with foliation
parallel to the sides of the bands. Sometimes little fractures or gashes extend
into the bands from either margin, and are filled with the material of the
surrounding gneiss. Often several of these bands occur close together, when
they are usually parallel with each other, as they nearly always are with the
fohation of the gneiss. The filling of narrow cracks and veinlets im the bands
is often coarser than the surrounding gneiss, but as these become broader,
and adjacent blocks are more widely removed from each other the filling
material becomes identical with the normal gneiss.

Several explanations may be suggested for the presence of these bands,
and these may be briefly considered. In the first place, they may be regarded
as indications of bedding in the gneissic series, in which sense they were
alluded to above. But their limited and irregular occurrence, as well as their
slight extent and sudden termination along the strike oppose this view.
Other objections will appear in speaking of the next supposition. According
to the latter, the bands are dikes intruded in parallel groups, and broken up
by subsequent pressure. At first sight this is a very plausible view, but it
seems to be completely negatived by the peculiar separation of the bands into
distinet blocks. Such blocks might result from faulting, but, in this case, no
faulting has occurred ; while, if the dikes had been separated by stretching,
the resultant blocks would have a tapering, elliptical shape, totally different
from that they show. It is impossible to believe that under pressure the
dikes would break into blocks, which would retain a rectangular outline,

while the surrounding. solid gneiss, under the same pressure, flowed around ~

SmytH—COrysTALLInE Rocks or St. LAwrRENCE Country. 49]

them. This happens, as shown above, in the case of limestone and gneissic
layers, but in the present case the rocks involved are too much alike to permit
the acceptance of such an explanation. This objection holds good against the
first supposition—that of interbedded layers.

The possibility of the black bands being segregations in an igneous rock
is, for the typical cases, excluded by their form, although it may be applicable
to some occurrences. There remains the supposition that the black bands are
fragments of an older gneiss, included in a gneiss of igneous origin. ‘This
explanation is the only one that appears to be in harmony with the facts, and
free from serious objection. According to it, the bands owe their shape to
their breaking from the parent mass, as they would, in the direction of
least resistance. Their occurrence in groups is just what would naturally
follow from such an origin, and the same is true of the irregular scattering of
these groups. The parallel arrangement of the neighboring bands doubtless
results from currents in the molten magma, which would tend to produce such
a result. It is probable that the breaking into blocks resulted, in part,
from strains applied after the magma was in a pasty and partially crystallized
state. The blocks were more or less widely separated, and the intervening
space was filled by the magma, which flowed around the blocks without
destroying their angular contour, and, at the same time, often produced an
obscure flow-struecture in the eneiss, parallel to the sides of the inclusions.
The fine fissures and cracks were filled with the more acid portions of the
magma, which were last to crystallize, and were strained into these cracks,
producing the coarser pegmatitic veins. These minor details, are not, of
course, im the least essential to the explanation, although suggested by the
phenomena observed in the field. The supposition as a whole accounts for
the facts stated, and has, as yet, no strong evidence against it.

The irregular black masses occur in much the same way as do the bands,
differing only in form and size. They are sometimes nearly circular, or
elliptical, but more often extremely irregular, with an outline marked by pro-
jections, and deep embayments. They often attain dimensions much greater
than those of the bands. The foliation is often pronounced, quite commonly
more so than in the surrounding gneiss. The two foliations, that of the black
masses and of the gneiss, range from parallel with, to perpendicular to
each other. Where the included mass is decidedly elongated in one direc-
tion, this is usually parallel to the fohlation of the surrounding gneiss. The
foliation, of the gneiss sometimes follows the sides of the black masses, as

though it had flowed around them, and not infrequently, narrow, irregular

492 Report oF THE StTaTE GEOLOGIST.

embayments in the blocks are. filled with gneiss showing this structure
parallel to the sides.

To account for the masses as anything but inclusions in an igneous rock,
is even more difficult than in the case of the bands. All of the phenomena point
to this origin, while they present great difficulties in the way of any other
explanation. It would seem, then, that at many widely separated points the
gneiss contains masses that can hardly be explained as anything other than
inclusions of some older formation taken up by the gneiss when it was in a
molten state. At some points the evidence is much more decisive than
at others, and while in the more obscure occurrences other explanations
might suffice, in the typical cases the one offered seems to be demanded.

From the foregoing it is apparent that the gneiss affords considerable
internal evidence bearing upon the question of its origin, and all of the
evidence points in one direction. To sum up briefly: there is the negative
evidence of the absence of all structures pointing to sedimentary origin ;
there is the uniformity of composition and structure over wide areas, with
changes by gradual transition; there is the common occurrence of massive
cores, In every way identical with plutonic rocks, and the presence of
structures in the gneiss that would result from the application of pressure
to such rocks; there is the existence of irruptive contacts between the
abundant light-colored gneiss and the less common, and older, dark gneiss,
together with the widespread instances of inclusions of the dark gneiss
in the hight.

While no one of these lines of evidence might be regarded as conclusive,
it is believed that, leading as they all do in one direction, their cumulative
force is great.

There still remams the external evidence bearing upon the problem;
and as this involves the relationship between the gneiss and the lime-
stone, this latter problem must of necessity be considered.

The absence of any sufficient reason for regarding the gneiss and the
limestone as portions of one series has been already pointed out. If
distinct, the gneiss is either older or younger; and in the former case the
relations of the two formations would shed no light upon the origin of
the gneiss, while in the latter they might afford important evidence.

No facts are at hand which prove conclusively that any part of the gneiss
belongs to a series older than the limestone, but this mere absence of evidence
can not be regarded as excluding the possibility of the presence of such an

older gneiss series, for, in the nature of the case, positive eyidence is —

Smytu—CrysraLLiInE Rocks or Str. LAwrencre Country. 493

difficult to secure. As already reiterated, there is also no evidence that any
considerable part of the gneiss is of the same age as the limestone; while
many facts are opposed to this supposition. As to the third supposition, that
the gneiss is, at least in part, younger than the limestone, there is positive
evidence, and of such a nature as to give, at the same time, abundant proof as
to the origin of these portions of the gneiss.

An example of this kind in Pitcairn and Diana has been previously
described, and need be only briefly referred to here. A large area of plutonic
rock, in some parts gabbroitic, in others syenitic or granitic, forms the southern
boundary of the limestone belt between Natural Bridge and Harrisville. The
igneous nature of the rock is shown not only by its composition and
structure, but also by the fact that it is clearly intrusive in the limestone,
cutting it along a very irregular line with the production of well defined
contact zones containing & variety of minerals.

The plutonic rock is often shghtly gneissoid and in thin sections generally
shows more or less cataclastic structure. Passing south and west from its
boundaries these features rapidly increase and the rock becomes a reddish
gneiss of medium grain. In itself there is no important feature to distinguish
this gneiss from other gneisses, its only exceptional feature being its evident
identity with the large area of plutonic rock intrusive in the limestone. Here
then, is an important area of gneiss, for which the two chief problems are
solved ; it is a modified plutonic rock, and is younger than, and intrusive in
the limestone. No other instance has been found where the phenomena are
exhibited on so extensive a scale, but facts similar in kind have been noted
at several points.

In the paper just referred to, it was stated that the southern border of
the gneiss area between the Edwards and Pitcairn limestone belts, was com-
posed chiefly of rocks undoubtedly igneous and intrusive in the limestone.
An effort has been made to ascertain the relations on the northern edge, and
in the one contact found between the two formations similar phenomena were
observed. The locality is about three-fourths of a mile south of the village of
Edwards. Here the gneiss is of the ordinary, rather fine type, which is so
widespread. Its relation to the limestone is clearly shown, and it is seen to
break through the latter formation with a most irregular irruptive contact.
As in the case of the Pitcairn rocks, there is pronounced contact-metamorphism
resulting in a formation of zones composed largely of coccolite, together with
feldspar, scapolite, etc. This locality differs from the first described, in that

it is the gneiss itself, and not the parent plutonic rock, which is in contact with

494 Report oF THE STATE GEOLOGIST.

the limestone. About two miles south from this locality, towards the centre
of the gneiss area, the road crosses a small patch of limestone only a few rods
square, entirely enclosed in gneiss. It would be difficult to account for this
as anytuing but an inclusion in an igneous rock, and that it is such, is further
indicated by the fact that it is filled with contact minerals. Thus, the gneiss
area between the Edwards and the Pitcairn limestone belts shows evidence on
both its northern and southern boundaries, as well as towards the centre, that
it is in part of igneous origin and intrusive in the limestone. The character
of the gneiss throughout the area is such as to render it highly probable that
this is true of the greater part of the rock.

About two miles east of the village of Colton, near the town line of
Colton and Parishville, the gneiss and limestone are shown almost, but not
quite, in absolute contact. The structural relations are not such as to suggest
conformity but rather the reverse, while near the c&ntact the limestone is cut
through and through by a pegmatitic intrusion. A characteristic contact zone
is present, showing coccolite with titanite, tremolite, etc., and the pegmatite
contains irregular masses of the same composition, doubtless inclusions of
altered limestone. The position of the pegmatite is such as to suggest that it
may be a secretion of a plutonic magma represented by the adjacent gneiss,
and this idea is greatly strengthened by the fact that the gneiss itself contains
coccolite masses precisely like those in the pegmatite, and very difficult to
explain as anything but inclusions of altered limestone. The phenomena here
are not conclusive but have value in connection with the facts shown at other
localities. Within a mile north of this point there are several recurrences of
structural relations suggesting intrusions, but showing no contacts. At one
point, however, which must be almost, if not exactly, on the contact, limestone
is shown with abundant large crystals of altered pyroxene, with other
products characteristic of contact action. An analogous case is shown in
Hermon, where, though no actual contact is shown, there is, Just on the line
where the gneiss and limestone should meet, a mass of scapolite, pyroxene
and other contact minerals.

The gneiss area north of Gouverneur village shows phenomena somewhat
similar to those near Colton. No contact is shown, but the limestone in the
neighborhood of the gneiss 1s often broken through by pegmatite. In this
case the limestone shows little or no alteration, but the pegmatite itself
becomes rich in titanite near the contact. The gneiss of this area also shows
abundant examples of the black inclusions, and of passage into wholly massive

phases,

Smyti—CrystaLLinE Rocks or St. LAwreNcE Counry. 495

The absence of any marked metamorphism of the limestone at its contact
with the pegmatite, is a feature observed at a number of localities in the case
of granites, and is of importance as showing that the mere absence of contact
products can not be taken as proving an absence of igneous intrusions. An
instance of importance is afforded in northern Rossie, where an area of rather
massive gneiss is clearly intrusive in the limestone, while the latter shows no
change, unless, perhaps, a slightly coarser grain than usual. The gneiss, how.
ever, is, like the pegmatite of Gouverneur, rich in titanite near the contact.
In the same vicinity, some two miles north of Rossie village, a rather dark,
fine rock, in part massive and in part a gneiss, breaks through the limestone
with an irregular irruptive Contact. At some points along the line of contact,
the metamorphism is confined to a zone not more than an inch wide, while at
other points great masses of pyroxene, scapolite, apatite, mica, etc., are found,
constituting an important mineral locality. The great variation in the amount
of metamorphism at different points does not seem to depend upon any
corresponding variation in the nature of the rocks involved. A probable
cause may be suggested as afforded by an uneven distribution of moisture,
the great masses of contact products being formed along channels affording
a favorable transmission for heated solutions, and, in some cases, doubtless
for gases as well.

~The two localities just described not only illustrate the variability in
the degrees of metamorphism but also afford further examples of gneiss,
igneous in origin and younger than the limestone. The development of
large masses of minerals in the last case naturally suggests the possibility
that other mineral localities of the region may show similar relations. As a
matter of fact, the association of minerals at many of these localities is such as
to lead to the inference that they have been formed by contact metamorphism.
In the case of the well-known localities east of Natural Bridge this was found
geested, although

ok

to be true, and at many other points similar relations are su
the structure is not so clear.

Numerous pits from which minerals have been collected in quantity have
been visited, and in nearly every case they have been found to be opened on,
or close to, the contact between gneiss and limestone. Pyroxene, amphibole,
scapolite, feldspar and titanite are the common minerals, an association which,
taken with their mode of occurrence, is highly suggestive of contact meta’
morphism. In most cases examined the gneiss is not part of an extensive
area, but is rather limited and more like a sheet. For this reason it often has

the appearance of being interbedded, thus making the structural relations

496 Report OF THE STATE GEOLOGIST.

doubtful. But, as bearing upon this, it should be said that it is a very
general rule in the region that intrusions of limited extent tend to assume a
form decidedly elongated in the direction of the strike, and, as a result, often
have the appearance of being interbedded, even where the facts clearly show
their intrusive nature.

The relations between the gneiss and the granite intrusive in the lime.
stone must be considered in connection with the question under discussion.

In the previous report 1t was stated that the granite often becomes very

Ley
fo)
gneissoid, so much so that in some cases it can be distinguished only by its
relation to the limestone. On this account no effort was made to separate
granite from gneiss in the large areas of the latter. As the gneiss has been
more carefully studied, the fact has appeared that much of it is quite as
massive as the granite, and decidedly more so than the gneissoid phases of
the latter. No petrographic distinction can be made between the massive
gneisses and the granite, a fact of much importance in the present connection,
for 1t at once leads.to the inference that the granites may be offshoots of
the gneiss, affording another indication of the origin and age of the latter.
The existence of granitic areas in the gneiss was not doubted in the previous
report, but it was felt that they might be of minor extent and importance, and
so it was stated that the explanation of the great gneissic areas as intrusive
must be employed with caution.

In addition to the facts enumerated above, many cases have been observed
where the structural relations of the gneiss and limestone are highly indicative
of the intrusion of the former, although the outcrops do not suffice to prove
conclusively such a relation.

The data presented in the foregoing necessitate the following conclusions :
All parts of the gneiss are not of the same age; some portions, of large
extent, are of igneous origin; of these igneous gneisses part, at least, are
younger than the limestone. These conclusions are merely the statement of
what is clearly and definitely proved ; but, with the facts in hand, some more
general inferences seem to be entirely Justified. Indeed, in the case of
extensive areas of the gneisses, positive evidence as to their origin and relation
to other rocks will probably never be found, and the problems can be
solved only by inference and analogy. Keeping in view what has been
stated in regard to the rocks, their uniformity, gradual transitions, massive
phases, inclusions, irruptive contacts, ete., scattered over widely separated
areas, it would seem that the following inferences may be drawn as, at least,

extremely probable :

Smytru—CrystauLuinE Rocks oF St. LAwrence County. 497

The gneisses constitute a complex series of rocks, differing somewhat
in age, and largely, if not almost wholly, of igneous origin; parts of this
series are clearly younger than the limestones, and while other parts may be
older than the latter formation, there is nothing as yet to prove that such is
the case. An exception to the latter statement is probably afforded by
certain laminated gneisses of limited extent, which appear to underlie the
limestone, perhaps marking the base of the series. This relationship, is,
however, inferred rather than proved.

If these inferences are correct,.-the task of mapping involves the
tracing of the limestones together with such minor portions of gneiss as
belong with them ; and, so far as possible, the differentiation of the gneisses
upon a chronological and petrological basis. As regards this latter part of the
work, it is questionable whether, in many cases, any very sharp distinctions
‘an. be made out, or definite lines of demarkation laid down, as the nature of
the rocks seems to be such as to preclude anything but rather broad
generalizations. It may be, however, that under careful study the present
difficulties will become less, and greater accuracy be attained than now
seems probable. Much that is now obscure will, without doubt, become
entirely clear when the whole area is studied with all possible care and detail.
Such a general reconnaissance as has been made serves only to prepare the
way for this more detailed study, indicating the problems involved, and
sometimes pointing to their probable solutions. The region is certainly
deserving of such careful examination as will lead to the preparation of an
accurate geologic map.

32

ae Bee

¥.,
<
c WY

3 «GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

REPORT ON THE GEOLOGY OF CLINTON COUNTY.

, ae JAMES HALL, H. P. CUSHING,
Bee ? State Geologist. | Assistant.

3 : ae 1895;

=

tS aues Hant, State Geologist,
> Smr:—Herewith I submit a report upon geologic investigations prose-

cuted by me in Clinton county.

Respectfully yours,
Hee CUSHING:
Western Reserve Universrry, May 15, 1896.
501

aN

<= ‘ude

‘ PAL? a p= c=

yatard iwc
ad ssi calaavan fuaprennap PpaphetegranantnplianpetE Dy aURRnG TA os. <setunemaneeenttataens)

eS ee ee ey a aaa

ek: oa, :
: conan N: prcdemat ey Abe pee on eee ae

cS | ohh

; , a

F
ape

ie

x fe
There el Ves WA EES ge 0
695 sare

Pew
, moo

by

fee nate

er >
ie area a ee aes ae Se cere

Ae ele at

ANT AINE HUM RIOR BHT AKIWIONE 5 teK02 KETMLID 40

(ay ay
A

hf wt hee:
Wy. roy ret the up ectiD Nhe nm

4
a) thes a

\

PLATE T

a 7 eficeNrreg

ABU}

2 fs
5 T i ;
KMS
aE E BEEKMANTOWN ~

es RUSSIA
PETERSBURGg PREDFORD

EWSW EDEN
Cambrian | Boundary
Pre-cambrian

. DT AUSABLE FORKS.

MILES.

MAP OF CLINTON COUNTY; SHOWING THE BOUNDARY BETWEEN THE CAMBRIAN AND PRECAMBRIAN FORMATIONS

Report on the Geology of Clinton County.

By. H.. P. Cusnine:

Conrents. Introduction, p. 503. Topography, p. 504. General Geologic Relations, p. 506:
I. Gneissic Series, p.506; II. Limestone Series, p. 508; HI. Gabbro Series, p. 508; IV. Paleozoic Series,
p. 510; Potsdam Sandstone, p. 510; Calciferous Sandrock, p. 512; Chazy Limestone, p. 513; Black
River Limestone, p. 514; Trenton Limestone, p. 514; Utica Slate, p. 515; V. Dike Series, p. 515;
VI. Pleistocene Deposits, p. 527. Metamorphism of the Pre-Cambrian Rocks, p. 529. Post-Ordovician
Disturbances, p. 5380; VYownship Geology, p. 581: Clinton Township, p. 532; Mooers Township, p. 532;
Ellenburgh Township, p. 533; Dannemora Township, p. 535; Saranac Township, p. 538; Black
Brook Township, p. 541 ; Ausable Township, p. 545; Peru Township, p. 549; Schuyler Falls Town-
ship, p. 552; Plattsburgh Township, p. 553; Beekmantown Township, p. 559; Altona Township,
p- 562 ; Chazy Township, p. 562 ; Champlain Township. p. 571.

The field work the general results of which are presented in this
report, was done during the tield seasons of 1893—94—95, about four weeks
during each being devoted to the work. On the last two occasions, Mr. M.
L. McBride, of Cleveland, at his own expense, accompanied the writer as
assistant and rendered valuable service. During 1895, a week was spent with
Messrs. Gilbert van Ingen and 'T. G. White, of Columbia College, in inspecting
the best exposures of the Ordovician limestones in the county, and Mr. van
Ingen’s palaeontologic ability was of great service in making clear some
perplexing points in the stratigraphy.

The entire county has been traversed and mapped, but only in a general
way, the desideratum being the acquisition of a good general knowledge of
the district before attempting the detailed work which will be necessary for
the proper elucidation of the perplexing problems which have arisen.
Furthermore, no good, or even fair maps exist of the greater part of the
county, so that, until such are available, it is useless to attempt closer work.
A beginning has, however, been made in the detailed mapping of the
palaeozoic rocks along lake Champlain, which is necessary in order to fully
bring out the structural features, and it is the present expectation to con-
tinue this as opportunity offers.

Since the report of Professor Emmons, over fifty years ago, practically
nothing has been published on the geology of the county except the

beautiful bits of mapping and sectioning done by President Brainard and
503

504 Revorr oF THE SratreE Growoatst.

Professor Seely. In addition to what they have published, President Brainard
writes me that they have mapped the lake shore southward from Plattsburgh.

It is hoped that this map will soon be published.*

ToroGRapny.

Clinton is the extreme northeast county of the state of New York, lake
Champlain forming the eastern, and the Dominion of Canada the northern
boundary. Its area is approximately 1,098 square miles. It lies entirely
within the St. Lawrence drainage basin, sloping for the most part to the
northeast. Close to the Franklin county line, and nearly parallel with it,
ranging northward from Upper Chateaugay lake is a pronounced watershed,
west of which the drainage is into the Chateaugay river and thence north-
ward, while east of it the streams flow to the northeast and east. Of the
larger streams emerging from the northern Adirondacks, the Saranac and
Great Chazy rivers flow clear across the county, while the Ausable forms part
of its southern boundary.

Topographically the county is separable into three well marked
divisions :

1. A hilly or somewhat mountainous southwestern portion, occupying
something over one-third of the county, constituting a part of the north-
eastern Adirondacks and characterized by their conformation; in other words
composed of massive ridges trending northeast and southwest, with inter-
vening steep-sided valleys of very variable width. Occasionally the ridges
trend east and west. They commonly have a rather gentle slope on the north
side, which is deeply drift-covered and heavily timbered, the rocks seldom
protruding above the surface ; while on the south the slopes are steeper and
often precipitous, exhibiting frequent vertical cliffs of considerable height.
The highest elevations in the county are Lyon mountain, 3,809 feet, and
Catamount mountain, 3,168 feet. The valleys are for the most part heavily
drift-filled, with rock exposures only along the larger streams. They some-
times expand into quite wide parks and are not infrequently occupied by
lakes, of which Chazy and Upper Chateaugay Jakes in Dannemora, and Silver
lake in Black Brook, are the most noteworthy.

2. A high-level plain, beneath which the knobs of the older rocks are
submerged, and which extends into embayments between their outlying

ridges. It has a maximum elevation of about 1,500 feet along its boundary
* Since the above was written the map and description have appeared. See Bulletin American Museum Natural History,
Vol. VIIL, 1896, pp. 305-310. The results agree with those obtained by the writer.

Cusutnec—GroLtocy or Crirnron Country. 50D

with the hilly tract, and slopes thence gently northward to the brink of the
St. Lawrence valley. The surface rock throughout in this county is the
Potsdam sandstone which les nearly horizontal, having but a_ slight
northerly dip, so that its descent is not greatly in excess of the average surface
fall. The covering of glacial material is widespread but mostly confined
to the depressions, and the numerous, often large, marshy tracts testify to its
irregularity.

The streams draining northward across the plain have for the most part
not channelled it very deeply since the close of the glacial period, on account
of the horizontal attitude of the rocks and their resistant character. During
the late Tertiary, the plain was much dissected by the drainage, but even
then the valleys were relatively narrow, the present summits of the plain
consisting of comparatively wide table lands of sandstone instead of narrow
ridges and mounds, ‘The new maps cover a portion of this plain in Mooers
and Altona and indicate that these summits represent portions of an earlier
base level, now tilted to the north.

3. A low strip along the lake, ranging from the lake level to an altitude

of 800 feet on its western border, and increasing in breadth going north.

From the 800 foot to the 500 foot level, the rise is quite abrupt, especially in
Chazy township, and the topography strongly suggests a fault, raising the
Potsdam on the west some hundreds of feet above that on the east, and
marking the boundary between the low strip and the high plain. Further to
the south, the heavy Pleistocene deposits largely obliterate this contrast.
This low strip is greatly dissected by faults, and to their presence its
minor topographic features are largely due. The fault lines are occu-
pied by marshes or small streams, while between them ledges of rock
project at all angles in a seemingly haphazard and at first, quite bewildering
fashion.

Throughout this low strip the main streams quite generally follow their
pre-glacial channels. The Saranac and Great Chazy rivers have channelled
out considerable valleys in the drift and are now widening them. The Great
Chazy river is in its pre-glacial channel throughout the low strip, exposing
nothing but drift in its banks. At Mooers village it leaves the old channel
for a short distance, and thence up-stream this frequently happens, but this
channel belongs topographically to the high plain. The Saranac is out of its
old course at the pulp mill, two miles above Plattsburgh, thence keeps to its
old valley till Cadyville is reached. Here a considerable gorge has been cut

in the Potsdam, but this is beyond the contines of the low strip.

506 Report or THE STare GEOLOGIST,

The smaller streams, the Little Chazy, Salmon and Little Ausable rivers
are wholly or mainly in post-glacial channels, and give little clue to the minor
pre-glacial dramage. Such part of the county as is most suitable for agricul-

tural purposes is mainly confined to this strip, and on it are many fine farms.

GENERAL GEOLOGIC RELATIONS.

Professor J. F. Kemp has recently published a resumé of the schemes of
classification which have been proposed for the rocks of the Adirondack
region, to which he has added a tentative one of his own.*

This, which comprises :

(1.) A basal gneissic series.

(II.) <A series of schists and gneisses with crystalline limestone.

(III.) Igneous rocks of the gabbro type.

(I1V.) Palseozoic sediments, lying unconformably on the first three.

(V.) Igneous. rocks found as dikes cutting all the foregoing, and

(VI.) Pleistocene deposits ;
will be followed in this report, emphasis being laid on the fact that it is
tentative, and probably simpler than the one finally adopted is likely to be.
The writer has elsewhere given reasons for holding that this scheme must
be expanded by the insertion of another period of dike formation between
(III.) and (1V.).+

As exposed in Clinton county these subdivisions may be epitomized as
follows:

Series [. The oldest rocks visible so far as known belong to a great
series of gneisses and are well shown in all the western tier of townships
except Clinton, and in Peru and Ausable. In their typical development they
are easily recognized. They present well-marked varieties, as below, all of
which seem to grade into one another,

1. Gneisses, commonly of red color, but also grey, brown, and other
shades, composed mainly of microperthitic orthoclase and quartz. Occasion-
ally these are the only constituents, when the gneissoid structure retreats
and a red granite rock results which seems to be merely a phase of the gneiss.
There has not yet been found in the county a granite which can be shown to
be intrusive in the gneiss, like that described by Smyth in St. Lawrence and

Jefferson counties.{ More commonly one or more of the minerals magnetite,

*J.F. Kemp, Report New York State Geologist for 1893, Vol. I., pp 444-447.
tH. P, Cushing, Transactions New York Academy of Sciences, Vol. XV., pp. 248-252.
{ C. H. Smyth, Jr, Transactions New York Academy of Sciences, Vol XII, pp 208 to 212,

CusHinc—GEoLOoGY oF CiiInton County. 507

plagioclase feldspar, microcline, biotite, hornblende and titanite are present in
varying amounts, and small apatites and zircons are almost universal. — Locally
a green augite also appears, but this is not a common occurrence in this
county. With the appearance of the more basic minerals the foliation of the
rock becomes apparent and increases in prominence as they increase in abund-
ance. Sometimes the quartz retreats and locally may be entirely lacking. .An
increase in plagioclase frequently accompanies this change, so that the rock
erades from a quartz-orthoclase into a plagioclase gneiss, often without
making any noticeable difference in the external appearance of the rock.

2. Widely exposed in Black Brook township are gneisses of quite
different appearance, and, judging from published descriptions of the Adiron-
dack gneisses, of an unusual type. For the most part they are very finely
granular, but alternate with numerous, often broad, coarse, pegmatite-like
bands. The fine-grained rock is of a prevailing lavender-grey or lilac-grey
tint, showing, when freshly broken, small, brilliant cleavage faces of feldspar.
It is quite free from basic minerals, hence foliation is not especially apparent.
The coarse rock is not unlike similar coarse bands in the ordinary gneisses,
but is more abundant here, alternating regularly with the other. There are also
present occasional thin bands of a basic gneiss weathering with a rusty hue.

In thin sections, both the coarse and fine varieties are seen to be made up
mainly, and often wholly, of microcline and quartz, the microcline having
almost universally a markedly microperthitic habit. Apatite is seldom absent,
and often abundant. Plagioclase and microperthitic orthoclase are frequently
present, sometimes in considerable quantity, and some slides show small
amounts of magnetite, biotite and hornblende, these being more plentiful in
the coarse bands.

Closely associated with these gneisses are others which, outwardly, more
nearly resemble the ordinary gneiss, and which have plagioclase for their
most prominent constituent, together with microcline, orthoclase, quartz,
magnetite and ferro-magnesian silicates in varying amounts. By their distri-
bution the impression is created that through them the microcline gneisses
grade into the ordinary orthoclase gneisses,

These microcline gneisses are in rather close juxtaposition to an area
occupied by the limestone series, and perhaps should be classed with that.
The thin bands of rusty basic gneiss interfoliated with them resemble gneisses
of that series rather more closely than they do the basic bands in the ordinary
gneisses. Aside from that indication the field evidence does not lean strongly
in either direction.

508 Report oF THE Stare GEOLOGIST.

3. Interbanded with the other gneisses, dark, basic gneisses occur, ranging
from an inch to many yards in thickness, and always parallel to the
foliation of the enclosing gneiss. They vary much in grain, but in general
are rather coarse, and are distinctly schistose in habit. When studied in
thin sections they at once separate themselves into two sharply contrasted
varieties, the one having the mineralogy of diorite, the other of gabbro. These
gabbroic bands are so precisely like the more basic portions of the gabbro
masses shortly to be described, that they should unquestionably be classed
with them and wiil be noted in their proper place. The other, and more
common variety is composed of plagioclase and hornblende with smaller, but
quite constant amounts of orthoclase, biotite and magnetite. Microcline is
sometimes present. Quartz may appear in small quantity, and in some
instances is found as inclusions in the plagioclase, and there only. Some of
these gneisses also carry much green augite along with the hornblende,
producing an intermediate rock between the dioritic gneisses and the gabbros.
In one specimen there is, instead of augite, a considerable content of an
orthorhombic pyroxene which is regarded as bronzite, the pleochroism and
double refraction bemg much weaker than in the ordinary hypersthenes of
the region. Measured extinction angles imdicate an andesine ranging toward
labradorite as the common feldspar.

As has been stated, the mineralogy of the rock is that of a diorite, or, in
some cases, of a gabbro-diorite, and its eruptive origin is regarded as highly
probable.

The gneissic series contains the workable deposits of magnetic iron ore.

Series IT, The rocks of this series consist of coarsely crystalline lime-
stones associated with certain peculiar gneisses and schists quite unlike any
members of Series L, and with other gneisses which closely resemble those of
that series. But one belt occupied by these rocks exists in Clinton county, so
far as known, and in that the exposures are few and meagre so that little
knowledge of the group can be obtained here, and the reader is referred to
Professor Kemp's descriptions of the numerous better exposures in Essex
county.* The Clinton county exposures are in Black Brook township and
will be described under the geology of that area.

Series LL1, This series is constituted of rocks of the gabbro family,
which are unquestionably of igneous origin and were intruded into the

members of the first two series. The main development of the rocks of this

*J.¥F. Kemp. Bulletin Geological Society of America, Vol. VI., pp. 241-262; and Annual Report New York State Geologist
for 1893, Vol. 1., p. 444

Cusutne—GeroLocy or Crinton County. 509

group in the Adirondacks, is in Essex county, where they have a greater areal
extent than all the other rocks combined, but they pass beyond the borders
of that county on all sides. Three outlying areas of this group occur in
Clinton county, none of which has been heretofore recognized as belonging
to it. The first of these is in Ausable township, extending north and west of
Keeseville, and is the direct prolongation northeastward of a great gabbro
ridge which comes up to Keeseville from the southwest. The second forms
Rand’s hii] in Beekmantown and Altona townships, is twenty miles north of
the last, and interesting as carrying the known Adirondack exposures by that
' distance nearer to the Canadian; further connecting links, if any, being
concealed by the covering of the later rocks beneath which they pass. ~The
third area forms the Catamount mountain ridge in southwestern Black Brook,
and Professor Kemp’s work during the past season indicates that the Whiteface
massive, Just over the border to the southwest, is a prolongation of the same.
The Catamount mountain exposures are difficult of access, and have not been
so thoroughly studied on that account; but the rock, while a little abnormal,
is unmistakable gabbro.

In their typical development the Adirondack gabbros, like those of
eastern Canada, consist almost wholly of plagioclase feldspar, mostly labra-
dorite, but ranging to anorthite, and to this very feldspathic phase Dr. F. D.
Adams has applied the name anorthosite. As the peripheries of the masses are
approached, ferro-magnesian silicates appear in increasing quantity, and ulti
mately the gabbros may become very basic, titaniferous magnetite, augite and
sometimes hypersthene being present in large quantity, together with garnet,
hornblende and biotite, these latter being largely, if not wholly, secondary.
With the appearance of these minerals comes almost always a gneissoid
structure in the rock.*

Though the Clinton county gabbro areas are of comparatively slight
extent, quite typical anorthosite may be collected from each, occurring in close
association with basic gabbro. Sometimes the ordinary gabbro contains
narrow bands of a quite basic character, of such persistence and with such
sharply defined walls that they closely imitate dikes in appearance. It is
more especially such bands as these, or larger masses of the same character,
that are quite identical with the bands already mentioned as occurring as basic
gneisses In the gneiss series, and which are to be regarded as dikes or apophysae

of the main gabbro intrusion which penetrated the gneiss from the parent

* For full descriptions of some phases of the gabbros, see F. D. Adams, Neues Jahrbuch fiir Min., Vol. VIII., pp. 419-497 ;
J. F. Kemp, Bulletin Geological Society of America, Vol. V., pp. 213-224.

510 Report oF THE STATE GEOLOGIST.

body. When not too finely granulated these basic gabbros show a tendency
to the assumption of ophitic structure. Such consist of coarse plagioclase
and nearly colorless pyroxene, both extraordinarily full of minute inclusions,
embedded in a granular matrix, in large part constituted of secondary min-
erals, garnet, biotite, hornblende and hypersthene with or without quartz.
The feldspar and pyroxene were apparently crystallizing at the same time,
for, while the feldspar is frequently idiomorphic against the pyroxene, it also
frequently includes the latter, while the reverse has not been observed to
occur. ‘These varieties commonly show beautiful reaction rims around the
magnetites, similar in all respects to those described by Professor Kemp in °
the Port Henry gabbro.

Serics IV. Unconformably overlying the older crystalline rocks is a
group of great thickness of nearly unchanged sedimentary rocks of Cambrian
and Ordovician age, which hides the older rocks from view over two-thirds of
the county. Unfortunately exposures are not always all that could be
desired, and in regard to a small part of the group the stratigraphy is not
clear. The whole is seriously in need of thorough palzontologic study, which
could not fail to furnish results of great interest and value. The group com-
mences at the bottom with the Potsdam sandstone, and terminates with the
Utica slate. No criteria have been found, by means of which an older
quartzite series can be discriminated from the Potsdam, as urged by N. H.
Winchell for northern New York.* The quartzites and quartz schists of the
Grenville series of Canada seem wholly or largely lacking in the eastern
Adirondacks, though they may occur on the west. Furthermore, they are an
integral part of the series. In the absence of fossil evidence, no division of
the Potsdam seems possible in Clinton county, though it is far from certain
that the whole is of Upper Cambrian age.

It is by no means impossible that rocks representing the Lorraine stage
of the Hudson river group have been deposited on the west side of
lake Champlain, but nothing younger than the Utica slate has yet been
discriminated,

Potsdam sandstone. The Potsdam is widely exposed in the county,
forming the rock surface in two townships and a large part of it in three
others, Out of the fourteen towns making up the county, there is but a
single one (Black Brook), in which this formation is wholly wanting. It is
also found at very varying altitudes. At Coopersville and in the Ausable
chasm it is close to the level of the lake, and at the former place the horizon

* American Geologist, October, 1895, p. 207, and Twenty-first Annual Report of Geological Survey of Minn., pp. 99 112.

GREAT

PLATE Il

a

WYNKOQP'HAELENBECK

SOUTH FACE OF SILVER LAKE MOUNTAIN, SHOWING ITS PRECIPITOUS CHARACTER.

PLATE III

WYNKOOP HALLENBECK CRAWFORD.CO

CHAZY RIVER AT THOM'S CORNERS; SHOWING POTSDAM SANDSTONE IN STREAM BED AND BANK OF

TILL.

CusHiInc—GEroLoGy oF Ciinton County. 511

is unquestionably near the summit of the formation. In Dannemora it is
found at an elevation in the neighborhood of 1,500 feet, and in Ellenburgh,
Beekmantown and Altona it runs nearly as high. Here, moreover, it is the
base which is exposed.

The color is very varied, from white through various greys, yellows,
browns and reds to even blackish appearing layers. Occasionally greenish
layers, appearing somewhat glauconitic, occur. In general the reds prevail in
the lower beds and are scarce above. The blackish varieties appear to be
characteristic of the summit.

The main mass of the formation is made up of quite pure quartz sand.
In the basal layers there is a large feldspathic content, mostly orthoclase, but
with a little plagioclase and microcline. Occasional grains of pyroxene and
hornblende and scales of biotite appear. In some layers zircon is prominent.
Garnet has not yet been noted. The basal conglomerates are often very rich
in magnetite. Toward the summit, dolomitic layers appear, regularly alter-
nating with those of pure sand, and forming passage beds to the Calciferous
above. Sometimes these are of pure dolomite, but prevailingly they are
sandy, and the rather large rounded grains of quartz embedded in a fine
mosaic of minute dolomite crystals furnish a striking combination in thin
section. These dolomitie beds are not, however, confined to the higher layers,
but occur sparingly elsewhere, even among red beds well toward the base,
strata of such an appearance that it would scarcely occur to one to test them
with acid ; in fact, the presence of these layers was first made known by
thin sections.

When the base of the formation is neared, massive conglomerates become
prominent, sometimes attaining great coarseness. They are commonly inter-
stratified with finer red, feldspathic, easily weathering beds, which are much
permeated with hematite. It is a curious fact that the materials of which
these basal conglomerates are made up are, so far as observed, always of
gneissic origin, even when the contacts are with gabbro and a considerable
distance from known gneissic outcrops.*

Along the lake these basal beds are seldom exposed, the contacts shown
being largely brought about by faults, but on the north they have great
prominence, especially in Ellenburgh (as noted by Emmons+), where they
have considerable thickness, but by no means make up the whole mass, as
stated by ‘hith. © H

* See description of a conglomerate near Keeseville on a following page.
+ E. Emmons.—Geology of New York, Second District, p. 309.

512 Report oF THE STATE GEOLOGIST.

A noteworthy characteristic of this formation in the county, is the occur-

rence of quite pebbly layers at numerous horizons from the bottom to the

top. The pebbles are almost invariably of quartz. At the base a few of

orthoclase are mingled with them.

The various layers of the rock show great variation in their resistance to
weathering. While the major part-of the mass is well indurated and very
durable, there are many layers in which the induration is much less, and
which disintegrate quite rapidly to a coarse white sand. The most unstable
portions are the red beds already mentioned as intermingled with the lower
conglomerates. These have a large content of orthoclase derived from the
gneisses, are permeated with hematite whose origin is uncertain, and break
down rapidly to a red, hematitic, sandy clay, which is a very conspicuous
feature along some of the roads.

The absolute thickness of the Potsdam hereabouts has not been
determined with certainty. As it was deposited on an uneven, probably very
uneven, floor, and as this floor was subsiding at the same time, its original
thickness must have varied much from place to place. The thickest section
susceptible of accurate measurement in the county, is that on the Ausable
river where, according to Mr. C. D. Walcott, there is a thickness of 350. feet,
with the base and summit not seen.* The impression conveyed by the wide-
spread exposures in the northern part of the county is that the total thickness
can scarcely fall short of 2,000 feet, and is quite likely much more. The
possible presence of faults increasing the apparent thickness, renders it
impossible to speak more definitely. If such are not present, the Potsdam is
unquestionably more than 2,000 feet thick.

While it has been impossible to make an exhaustive search for fossils, a
sharp lookout has been kept for them, and considerable time spent in the
quest ; yet none have been found except along the Ausable, where their
presence has long been known. The Upper Cambrian age of the higher
portion of the Potsdam has been shown, but there is as yet a complete lack of
paleontologic evidence as to the age of the lower part.

The Caleiferous sandrock, Rocks belonging to this division are spread
over a considerable area in the tier of townships along the lake, but are
unfortunately so concealed by Pleistocene deposits that the Potsdam-Calcifer-
ous boundary is almost completely obscured, and the Calciferous exposures
are often disappointing, though excellent sections are exhibited im Beekman-
town and Peru. Professors Brainard and Seely have carefully studied the

“Cc. D. Walcott, Bulletin 81, United States Geological Survey, p. 343.

Cusuinc—Geronocy oF Crinron County. 513

Calciferous of the Champlain valley,* and their section at Shoreham, Vt., gives
to the formation, which they separate into five subdivisions, a thickness of
1,800 feet. How large a part of this thickness the Calciferous possesses in
Clinton county, can not be determined, but commonly the different exposures
are correlated without difficulty with the various members of Brainard and
Seely’s section. The basal layers of the formation are shown in Champlain
township, conformably overlying the Potsdam. In Peru and Beekmantown
are good exposures of the higher and more fossiliferous members. The lower
half or two-thirds is made up largely of grey, often sandy dolomites, quite
barren of fossils. In the upper third, beds of limestone are mingled with the
dolomite, and some sandy beds, weathering with thick yellow sandy crusts,
also occur.

Chazy limestone. At Chazy village is the type section of this group
which follows the Calciferous in ascending order. Brainard and Seely have,
however, shown that the lower one hundred feet is lacking here and that the
Valcour Island section is more complete.+ Besides the excellent exposures in
Chazy township the rocks of this group are also well shown in part just north
of Plattsburgh, and on Bluff Point, two miles south of Plattsburgh, extending
thence to the south into Peru, where the lower part of the formation is better
shown than at any other point in the county on the mainland.

~ Brainard and Seely have recognized three subdivisions of the Chazy
rocks, and their detailed section at Chazy village is reproduced on a later
page. The lower subdivision is largely constituted of quite crystalline lime-
stones of grey color, often full of crinoidal fragments and with Orthis costalis
the most abundant fossil; the middle division is of blue-black fine-grained
limestone and contains Maelurea magna at nearly all horizons; the upper
division is quite variable in character, but is largely composed of somewhat
impure blue limestones, carrying Léhynchonella plena abundantly.

The aggregate thickness of the Chazy limestone at Chazy village is 740
feet, with the base not shown. On Valcour Island, Brainard and Seely give
it a thickness of 890 feet, and there it seems to reach its maximum.

For the most part these rocks are easy of recognition, and even small
exposures may be assigned to their proper position without great trouble.
There isa considerable quarry enterprise engaged in working the rocks of this
group, some beds furnishing an ornamental marble, some a rough building

stone, and some being burned for lime.

* Bulletin American Museum of Natural History, Vol. LII., No. 1, p. 3.
t Bulletin Geological Society of America, Vol. IL, pp. 293 to 300.

30

514 Report or tHe Stare GEOLoGIst.

Black River timestone. The massive dark-colored beds of this rock are
well exposed at numerous points in Chazy, directly overlying the Chazy lime-
stone ; but outside of this township it is not well exposed. It has a thickness
of thirty to fifty feet and is a brittle, black limestone with conchoidal fracture.
Columnaria alveolata is its most characteristic fossil, but is here confined to a
single stratum a few feet thick, at about fifteen feet above the base. Above
this is a zone with abundant large Maclureas and large masses of Stromato-
cerium, both of which are closely like the corresponding forms in the middle
division of the Chazy, so that, unless care is taken, the two may be con-
founded, as was done by the writer in one or two instances. On smoothed,
mere surface exposures the resemblance is very striking.

Trenton limestone. In Chazy and Plattsburgh townships are excellent
exposures of portions of the Trenton. In the bed of the river just east of
Chazy village, 150 feet are exposed lying on the Black river limestone. On
Crab island, about 200 feet in thickness is exposed, the larger part of which is
above the horizon of the beds at Chazy, while the lower fifty feet corresponds
to the upper part of that section. The two together give a thickness of
about 300 feet, but the summit is not shown. The faunas are being studied
by Mr. T. G. White. In general the lower half is characterized by a brach-
iopod fauna, some bands being crowded with shells of Zeptena sericea and
Orthis.

The upper one hundred feet of the Crab island section holds a lamelli-
branch fauna, with cephalopods and trilobites, while between the two is a
zone with a sparse trilobitic fauna.

This lower portion of the Trenton is mainly made up of black, ringing,
somewhat slaty limestone, the different layers presenting much variation in
the latter respect.

In northeastern Plattsburgh, and extending into southeastern Beekman-
town, occurs a series of black, quite slaty, calcareous rocks, which are excel-
lently exposed on Cumberland Head. As there exposed they have had
developed in them a slaty cleavage at a high angle with the bedding, which
has already been described.* In Beekmantown this is not so pronounced, but
is present. No base nor summit to these slates 1s exposed, and the strati-
graphic evidence concerning their position is not decisive, but points strongly
to their being of Trenton age, or, rather to their not being older than the
Trenton. As the Chazy and Crab island sections furnish us with the basal

300 feet, and as there is an unknown vertical interval between the two, these

*H. P. Cushing. Report of New York State Geologist for 1693, vol 1, p. 483.

Cusuina—GroLtocy or Curnton County. 515

slates must be well up in the Trenton. It will be impossible without pro-
longed study to arrive at a just estimate of their thickness here. The apparent
thickness on Cumberland Head is very great; but there are also evidences
there of much disturbance, and it is strongly probable that there is repetition.
In addition to the evidence afforded by the slaty cleavage, one or two faults
are plainly visible in the slates, and the topography strongly suggests others.
Yet, taking all these things into consideration, 200 feet would be a very
modest estimate of the thickness here displayed, and double, or even treble
that amount would most likely be much nearer the true figure. The entire
Trenton in this vicinity, therefore, must be very thick. The writer had the
pleasure of conducting Mr. van Ingen to Cumberland Head, and to the ex-
posures of these same slaty rocks in Beekmantown, and since the above was
written a letter has been received from him giving the results of his study of
their fauna. He pronounces the horizon to be high up in the Trenton, and
with features in common with the “ Quebec group” of Canada, so that it may
turn out to be more nearly allied to the Utica slate than to the Trenton
limestone; that is, the Utica as represented in Canada.

Utica slate. On Stony Point, in Champlain township, is an exposure of
black, ringing, much-jointed calcareous slates, the joints largely filled with
crystalline calcite, which carry the ordinary fauna of the New York Utica
slate, Zriarthrus Becki, Climacograptus bicornis and other graptolites, and
Endoceras. With the exception of this single exposure, shut in on the east
and north by the lake, and on the west and south by a marsh along a line of
fault, no rocks known to be later than the Trenton limestone occur in the
county. The Utica slate is also exposed on the east side of Isle la Motte.

Series V. The various types of dike rocks occurring in the lake
Champlain district have been described at length by Kemp and Marsters,*
and would need little mention here were it not for the fact that their
study in Clinton county has emphasized certain facts regarding their dis-
tribution, which are not so apparent in Essex county and along the lake.

The dikes are readily separable into two classes; black, basic dikes of
the varieties known as diabases, camptonites, monchiquites and fourchites, and
lighter-colored acidic dikes, closely approximating the same type, and known
as bostonites, the term being applied to the dike-form of feldspar porphyries
or trachytes.

The acidic dikes known in Clinton county (twelve have so far been

found) differ considerably from the typical bostonites as found and described

* Bulletin 107, United States Geological Survey.

516 Report oF THE Sratre GEOLOGIST.

by Kemp from along the lake.* Those have a prevailing light tint, creamy or
brownish white or chocolate, and nearly or entirely lack magnetite and ferro.
magnesian silicates. The Clinton county dikes, on the contrary, are either
red or mottled dark red and black, or purplish grey in color (one is nearly
black), and with one exception contain considerable amounts of one or
more of the minerals, magnetite, biotite, hornblende and monoclinic pyroxene
in the ground-mass, and dike No. 9 even has porphyritic biotite. Some of
them have a pseudo-schistose appearance. Most of them have porphyritic
orthoclase, and this mineral makes up the main portion of the rock. The
ground-mass has a trachytic structure, most marked around the phenocrysts.
In these last two respects they agree with the typical bostonites, and they are
not necessarily more basic because of the greater prominence of bisilicates, so
that they are regarded as bostonites varying-somewhat from the type, and
seem to represent an intermediate stage between these type bostonites and the
“ oranite” dikes described by Marsters from lake Memphremagog.+

Professor Kemp,-some time ago, called attention to the fact that the basic
dikes are more numerous in the Pre-Cambrian rocks than in the Palaeozoic
series,} and further, in discussing the relations of diabase and camptonite, to
the confining of. the diabases to the former, and of the typical camptonites to
the latter rocks. Many of the diabases of the region, however, grade strongly
toward camptonites and augite-camptonites, and in two instances of this sort
in Clinton county, the dikes are very narrow and seem almost certainly to be
off-shoots from large dikes of typical diabase near by, recalling the camptonite
apophysae from a laccolite of diabase described by Brogger.

The diabase dikes are found abundantly throughout Clinton county
wherever the Pre-Cambrian rocks are exposed. The camptonites, monchi-
quites and fourchites seem to decrease in number north of Port Kent, and
north of Plattsburgh are wholly lacking, in so far as negative evidence can be
depended upon. This peculiarity of distribution, coupled with the fact that
all along the northern line of contact between the Potsdam and the older
rocks in the county the diabase dikes are found numerously on one side of
the line and not at all on the other, has led the writer to elsewhere express
the opinion that there were two periods of dike formation in this vicinity,$
one preceding and one following the deposition of the Paleeozoic rocks of

Series IV. The diabase dikes belong to the earlier, and the bostonites,

‘These differences have been noted by A. 8. Eakle, who described the first bostonite known in the county. American
Geologist, July, 1893, pp 32 and 33

+V. F. Marsters, American Geologist, Vol. XVI., pp. 25-29.

t Bulletin 107, United States Geological Survey, p. 27.

§ H. P. Cushing, Transactions New York Academy of Sciences, Vol. XV., pp. 248-252.

Cusutngc—Gronocy or Crinton County. 517

monchiquites, fourchites and camptonites to the later period; though on

9
account of the facility with which the diabases and camptonites shade into
one another, it may not always be possible to determine to which of the two
a given dike in the Pre-Cambrian rocks should be referred.

The diabase dikes are very common and widespread. Scarcely an out-
crop of any extent of the Pre-Cambrian rocks can be found without disclosing
the presence of one or more of them. But, as was to be expected, their
distribution is irregular, as they are only occasional in certain areas, whereas
others are fairly seamed with them. Sometimes a veritable plexus of dikes is
exhibited, anastomosing in all directions, enclosing great horses of the country
rock, and so variable from place to place that no satisfactory generalized
measurements can be made. The most notable example in the county is in
southeastern Altona township, where the Old Military road crosses the north-
east spur of Rand’s hill. Cutting the gabbro here is a grand exhibition of
dikes, which will be more fully described under the discussion of that town-
ship.* Another striking exhibition of dikes is found along the west shore of
Upper Chateaugay lake, and yet another on Dannemora mountain.

Appended is a tabulated list of the dikes found in the county by the
writer. Kemp has noted the occurrence of others in the Lyon mountain iron
mines, and two from Palmer hill, and three others have been described

by Eakle.

*See E. Emmons. Natural History of New York, Geology, Part II., p. 28.

Report oF THE Strate GEOLOGIST.

518

*sqsKsn0u0yd osvpoorsed
pur ogtone ‘ourarpo on wdsqdiog

‘YIP O]SuIs BJO
peogsur snxeld eyIp eTqRaea VW

“45 SL
jo jipta vw Surt{dnoovo oop
oll ‘sotpouraq [BeAes JO suxe[d
oyip vy ‘olwdydiod Aposavog

‘OIQGVS YY
UL oOz-IROYs v 4nd ‘eyIp B ION

*posodurosep you,

*pRod Oy 9B Joos Pp poypuLy

‘poyrvur [JOM Jou ing
-onajs oy Ayourp ‘ssBui-punois
ur episdorp pur oyyrde
aimos ‘oytgo1g Tou ‘eg1o1g
pure osepoqjyso yo sysfao0usyg

‘soqouraq sq1 Aq dn 4ipds [le st
OLG VT OYA SpavVA OG] JO [IPA B
IO *S9g osed uo poqisosop oy

“IPI TAO S}I OF POgTNLF ST

‘OyLOTTO oulos puke eyMeMoy
e[qeiepisuoo sey ‘orgaAqQdaog

*poesoduros9p oye)

ASVGVIP OUIATTO

OSUGRIP OULAT[O.

OSUGCRIP OULATIO

(8)

Scho Os CC ek(n

Se es SEERA GL

sere" = QI1LLOJSOg

2”) °=s >: SOSUelGn

“-"""> 9q1rmoysog

"o>" 99> ogBqRIC:

=o os se mes ace cc

oIqqey

OLQQBY

OG Qe

oI1gqey

OIG Vy

org qey

er

oOIgqey

orqqey

OAGQeRy

O1g.quVry

i.e, SSICUE):

“Ol

“HL 008 ‘S

“H 00S “N

“OL 009

“H 009 ON

“tL 009 “N

“H 008 “N

“SMUV IN

“INV NT

“STIV AM

“ULOT "WS
+959

+ US

“WF ST

“UlLZ “WS
ULF 8

“Urge “J OT

+ “93 OF
Maney Meee
Ulg “495 ¢

Beh a

“HLTA,

Pah | wee etl ca ONG LOCO ay,

cerecers CT ‘ON JO GJ10U Jooy OG

“77"""""Neod JO opis ysvo oy
wo ‘TT ‘ON JO ysvoqynos 0/491, V

“peor ol} dorveu yeIpMoulos
pue TI ‘ON Jo YQ10U spavd 0Z

Hos => -s === nOBITOO ULBPSs}Og,
| -o1qqey Suope wees []eus
jo Yynos spavk Op ‘osnoy
|-[OOyOS JO yseMTQIOoU opTU 4

““-""--@ "ON JOOS jo [INOS
Ivy jou ‘oyiduing soavo]
Hy s§,pary dn ourl oso My

"*"" pRod JO opis 4sve UO Sut
-MOYS ‘OT “ON JO Ygaou spavd OT

Fie michele Sie -1 DUOd TOM geo
‘,°ON puosoqg spavdk Opp sursog

‘ON JO YQuou spavt OTT Speror-Ag

Pip ee tedenieie Og 2) ales saaGrONETO
yynos spavdk gg ‘prox Jo ysaAy

Brey OE oe Saas ChON@E OT
-SIPOOYOS “ysomygiou Suis |

‘oytdaing Aq [LU spury jo
espo UO oinsodxe sslous 4SIiy |

*ALIIVOOT

Tk oa SOOTY:

7 eon Ty

OE We So CUOLIYT:

De am ER ELOY

Pie BOOTY:

oot ea UOT ys

oe nee ems LOE Th

PIED SOCOM ALON Np

“27> =5"= BUOITY.

oP Sheet a RUOULy

= Siepists -* BUOITY

"dIHSNMOT,

|
|

ST

las

IL

or

i~

G EOLOC

YLINTON County.

Yer OE,

7

CusHING

‘SUOTJOOIIP [[B UL SuLtBoq

soypuvaq TRUS JO YIOMJom Wj e OSEOCIC a |simin eee -- orqqey “OL 00S *S CY Gr Aa eae seciee Q9 ‘ON Uorpaey |
qou ‘esnoy 8,ose0y “Apt JO You |------ erqeg uy | eor
~orisydaiog |* esevqvip euralg |*7777" 77777" sstouy “1 009 "N || “UEg 379 | O[[LAUOZUITD JO YQ10U peor uO |
asnoy 4siy Jo YQIOU spares OOT |77>7 77° aTqug ny | og
*ssvUl-puno1s |
Ul 98pueTquI0oy WMOIq oUIOS | |
pur ey yorq qouur f;epropepsfury |-->-~ SOS AIR TO ACG (PPP P SOF OILS ez} yak |) “HT oAG'’N | “UIQ “9 § | ~-"-"7777°"* por zo ysou gsnl
| OTfTAUOZUT[G Jo YZtou epru § |---->- erqeg ny | 6L
2 OS COURS S 3 Se ICO RB ACS OE SRP OS OSES | OIG OSBqBIC? ||*-=---==*i=°= ssTeus “OH 0f9 °N SUTIG SS nee olr's sissies oT [LATOp AITO
| jo ysvo ysnf pvor aoata Xq osopg |------ aqeg ny | gL
SHIGRS 3H 25) OGD OO DOR OFAC pomorselseiaiiliso=i\-/s Sk ORE CBT Gn lhe mee anne AS TOUL) “HE 009 °N 43% | SL oy JO ysvoyjiou spavd QOZ |------eTQug Ny | Ly
SOUMCATT ALOT | ees ae esBqBIq |----"---"°" o1qqey ‘A o0L N UTC (sc 0Z (999 {pBor IOATI 0
98O[O ‘oT [LAGSeO Y JO SOA SoTIUT
tz ‘pueq siq ye yurq aoa -77--* erqeg ny | OL
‘pesodmooep qonut formadydiog |- oseqeip outarto |*--7" "7777" orqqey Teese awe |) Cee; cage [poocncopee 9) ‘ON OXI JO 1s¥9
opi F ‘ayes [[0] ye por IwoN |---->- aqeg uy | ey
‘pesodmooep Apysiyy | -7- >>> (4) osequiq |----" SS" O10Q 8x) ‘A 008 “N ‘43 | "7°" *pBor Jo yQnos sprvd COT |
pur ‘o[[tAeseey jo ysom ‘G
ON [OOO Jo ysvoyynos opr fF ~~~ ~~~ aqes NY | GL
sere secee De GRRRC OLS OOS ICR OBA Yh <1 7013) (4 (a ieee CO a CK (2 9) ‘A 008 °S TOG Wille cinen pee areas se ROT ONG!
-qvs jo 418d ysvoyqyiou ouleIyxm |*-----eTqeg ny | 69
‘oy 1m0yd erro |
ay1sne sopovoiddy ‘opi ‘UlcT
yore soyouraq porpered omy sep j-777 7 77> “eseqeiq |°---~ GOES Th (C039) "HT oS (S| ‘ULG “93 G | ~"-"esnoy soseoy ‘Ip_ Jo Hoe” |------ erqeg ny | 39
*‘posodmovaq |--""---- COSCO GLC ee nem cues OLAGU) ‘A 008 "S| “US “FE | --- LON ONT JO YJsOM spaws g j-------- eaoylTy | 8T
“YoRo JOO T JO :
wy JO omg ‘soyourarq ory} UY |--77 7777 -esuqeiq |----"*"°77> orqqey "| O09 'N | “GLOL 9E F | ~---ouey, du zoqqany spavd Oat |----77** euOgTY | ZT
sisfoieia’eo\nninlm pete ain te alee gece hal SocicRslo SONU s | rs ae a sarc OL Cie k) "a oGZ N Bil at? al Hp iterates oa --gsnoy-[ooas
jo qjnos ysuf {pq s,puey
Suipuosose ‘oue, dn oytur F |-------- RuoifTy | 91
‘SMUVAGY ‘AVN “STIVM. ‘HULLS “HLTA, ‘ALIIVOO'T *dIHSNMO, ‘ON

LOGIST.

O

1D)

Y

\
STATE

PORT OF THE

=
vi

Ri

520

*paurezgo oq Oo}
[vlioyeur yseay Lava fouraecydiog

*SUOLS

-IATpP (MOF UL SVM Toes OTOL AL

‘oyraojgduies
eyisne Surqovordde posolg

‘quo Surqourd qoq
‘punoy saqourrqg [[vuUIs OMT,
‘oqruoydures o91snv Sarqovorddy

*pesodxo
[Je Jou pue pesoduoovep ATpeg

‘OANJONAYS MOY JUET[II
“XQ ‘SSBUI-puno1s UL SepuoTd
“10 UeeLs = T[RUIS — SNOLeTT
“NU PUB OPTOUSVUL o[Qv1apIsSuOD

‘sqsAroouoyd osvpooryy
-10 SBJT ‘oUTUOYSOG vB OF OISLG
Aiwa Ssuvoddy pur fepualqusoy
UIIAS PUB OPLIJOIG ONT SUIeyUOD

: *posodxea
Ajaood pure ‘posodurosep AL StTyT

‘apuel[qux1oy pur
OLIJOUSBUL SUTRZLOD “YANOS ety
01 “AF 9 por[NeE St FLV Asvo oy}
fvonyins oy} ye posodxe qooy ZT

*SSUUL PUNOLS 9} UTOPUY]( UOT
jo Junoue T[VuUs B pu ‘syshao |
-ouayd oytsue osavds sureyu0p |
|
‘SSUUI-pUNOId ULOITIOIY |
pue opustquso0yg foyisne fsysdao
-ousyd esvpoyyio ose, A104

Ser Gb

“== == -9Seq er

“OsUuqul(y

qui

---(4) oseqruig.

--> > oJ LUO4YSOg.

~ (4) op tMOysog

nea oe osBVeqeld

“77> oy 1UOysog

-77 > og1uoysog

9110 SOG

“OLIN NI

se tee tee eee

SSIOULY)

sslowy

ssTouy

SSTOUY)

sslouy

SSLOUD

SsTOU)

ST ee oti a 5.9)

Sand w asaaiee Ones)

Seen meme te OCC)

“STTV AA

“Hl 09 “N

“tL of9 °N

“A 009 “N

“MH ofl *S

(i)

“Hd 008 *S

“H 008 “N

“WS 9

‘Urg "4

in]

“Ur OT

“WT

(i)

UlG “WEE

“Ul OL “I T

459

“FF 0G

"HLAT AY

“"-" $8 ‘ON JO JSva Spor [BIVAVG

-----""73 ‘ON JO 48vO Spavt Qe]

PRIS OOOO IS OT MLO HH COCO)
SyIOF ofqrg ny jo ysvo gsul
o1nsodxe sslous UL OYIpP sity
Feisiapie\sia nici = ii (* OUT ANON:
aTqVy uy Jo Jsem opium ¢ ‘9
‘ON [OOO JO YJzou spaeV’ YQOZ

"TTT TT TT "LZ ON OFC 04 0801

PSE RS SISOS Caja (aereyyyy 40) Le (shaKays
soplur ¢ ‘peor Jo giurutns Ivan

sores os5s 5 Ss UdplOx) «1 IVON

Tele ae re me ee, MLO Ter ON:

“+77 "" "97 oN Jo WQaOU spavd (pF

§.1osuvg ‘ayy ive YI spury

PBOI UOT FSO OTLUT } *y Jorg
-sip Jooyog jo qavd ysomyy10N

-- yooig your

“> yoolg ovlqd

“- yoorg souvlg_

“* yoorg Yourg

“UMOTURUTYIIG

“UMOJUBULY II

“UMOTUVULY 99

“UMOTUVULY 90gF

|“ UMOQUvUTY ae
|

|
|

“UMOTUBULY VO

“UMOJUVULY OO

“ALVIVOO'T

t8

£8

FOL

€0L

1g

0&

6G

8G

“ON

GroLocy or Crirxron Counrry.

CusHING

‘SOPLOTTIS UVISOUS vUI-O1LOF
OU Jnq ‘oZIoUSVUL oT YRVLEpIsMO;

*pesodmovep qonuyy

‘sgsXroou0yd osvpootsud osary

‘oplopeure f opuelquioy ou
Sqguonuboapur ouLarlpo feqWeusvUt

pue agorg YIM ‘suolyRieues
OM} UL OJLSNY ‘jeplopepsAuy

‘oovtd ul dees goN “dump wow

*posoduioos0p ATpeg

*pesodmooop ALywory

ora Aydaog

‘quyqy Jo qouesq
: K(quqoad puv ‘6g ‘ON 09 1eTTULIG

; ‘og aojdurvo
ejione Suryovroardde Ayposolp

“sory
eqyib fsysfiooueyd oytsue osieryT

‘SSlOLS JO Sos1oy, popupout Au

ee ae O94yLUOso,

STS SEA LG [

Sa --" -asuqviqd

===" - “Og OINO WT

-OSVQGLIP OUTATLTO

S550) -) OSV RIG

nas OS OER

Par ey AO GY

nahn SOS UCL

Sie ae “* -osVeq Bil

SP Galt rs “OSBGRVICT

|" OSUGCVBIP OVUIALLO

[-="" "=== -9suqviq

“AINVN

Tih shee eS LOU)

|
|

|
/-9UOJSOUTT WOYUOLT,

\ eet Bem & > SST@U‘)

vos ah Te = SHTOUR)

TIT TTFF T= OI ger)

ite Meer oe a) KS SLOT)

Pa o> eek eet DOS LOUL SY

vse > oF edie pate | LAS 3 |

ade Gyre aes tn SSlouUy)

Bietae te aad BSTOTILX)

Re ie at ae SStOU4)

“tL 008 N

mC f

“H 002 'N

(4)

(3)

“A 099 "N

“H of9

“A oS

“H 006

“dH oS

“MTEL

w

N

‘'N

‘ul

ILL A

Fee nioueuuRd JO You
opi Furey unou viomeunE(T
I9AO pvor Aq oes OFIP ISI

pe ie AIO OT 0 Cay =a (0
WOyUI[D JO yorq gid Fo [TVA uy

BODE SOAb aXOnKOL
es00[ UL puRIst Jo puse qQnog

ak ae PARDONS OOS Fy oe (Hea Hf
“TIM. Ivou peq-o10 ousog ut

“Iq SoM YITM Toounl saoqe
ojlur F ‘yung gsom uo ‘IOATI
IVUBIVG JO Youvrq yYnos Ag

“=---pvor Jo YQuos sparvd Moy
ve ‘qysanqdvpy JO gsoa ofiut F

pele here sini “"7gp ‘00g fs,prer0s
“ZY “AJ JO JSOM SpoOL MoT VW

“757 57> 99 “ON JO [Anos spavd )

“"--yoo1q yortg_ saoejue puod
YSsnig Jo JoTINO 919A ‘peor Kg

“-""Q8 ‘ON JO YQUOS spor Moz
vB ‘peor UL YAOF JO YJLOU ysune

BESS Mr TG Ea os Seer es wOOTe
jo opis ysvo ‘oSvT[IA yooug
yorrqg jo yjrou ysnf peor Ag

SS OAS) 2 SOO DOK > Baye (
oy Jo ysvo ysul ‘TaAtr Suope
sdoiogno ssious Jo pue 4svo yy

“"* BLOW OUR (T

aa P.LOULOUMLG (T

[-"* BlouleuUed

“*" puRisy quid

“- yooug, your”

“- yoorg your
“> yoorg youl

“> yooug youl
-- yooug your

“= yoorg youl

“> yoorg your

"7 yoorg youre

“- yooug xorg

“ALIISNMO JT,

FZ

06

61

98

‘ON

TATE GEOLOGIST.

S

ReEporT OF THE

ip
~
>

Te)

*‘posodwmooo(T

*posoduro0eqd

*<poq-o10
ogg Aq poyooye sourpvas sseduoy

‘a10 OYJ F[NVF JOU Seog

‘OSUOOLS
-ejd omos Ajgueardde feyisue
Jayye Aavpuooes opue(qusloy

OMOS {SNOISNPOUL SB ej yorg pue
aepuelquaoy Gonut : poropoo-yauqg

‘OyIHuB OI
-Aydtog “yooy OGIO GIPIM & IOF
SUOLJONOIIP [[B UT SSIOUS og SULvEg

‘opuald
-ULOY PUB OEF1VOIG eTqQBAIopIs
-u00 = Sasepooyqauo = orga Ay dao g

‘qouraq B A[QBurnselg

*posodurosep tonut £10 4

“SMUVNGY

J--> >> -Gscqurc
page asuqei(
“OSUGBIP OULAITO
Soacine- OUR dEtCT
a sisil= =" 99 BC BIT

i ein) eee ON CCLELG)

-oseqeIp OULATTO

rer ON GOIETCT

ny wh meme KG f

Soe ONS aL,

-asUqeIp OUIATTO

“=--="= 9g 1TO1sOg

$2 te OSCR

v7" > (4) osequiq

Pe Boag osSVqgel(y

“TINW N

oe es 5 “77> sstouy)
ssTouy
Sslouy
ss1oud
sstouy

sstouy

SSTOUy)

SS1OUy

sstouyy

ssteuy

Sele)

hie Waal 7 9 SSIOM)

SsTouy)

SSTOUX)

ss1ouy

“STIVM.

(4)

“tH oO¢

“A 00S

“A 00S

“HW oGS

(i) “Hl

“a

“HH o€$

“TH oSS

act

“AMEELG

&
Lex}

=|
bon
s
ol
a

(4) “44.0

+95 ST

(4) 39.9

"Ul 6

MIG “OF
+45
“HLTA,

“--=" OG ‘ON JO (JOU spava QOE
“----* 9G ‘ON JO Yyatou spaBdt ey
GG ‘ON JO YQa0u spavt ec
"7-7" $G ‘ON JO YAO spavs Gg
“--7-"" eG ‘ON Jo WQ10U spied 6
So SPeeeS Pee eSrir sre se Omey
Avsnevoeyg roddy jo proy
qv eprs[{iq uo gyno peoaqrer
AvSnvoyeyD jo pus qynos 1v9ON

"7-77" 7G ‘ON JO 4¥sOM SpAlVA YNZ

"77" *""QG "ON JO ¥SOM SprvVd JT

BSS ACO OCS Goo ore Gy)
uregunom uodry 09 osoTo gid
-010 JO pmo ysea puodsoq ysn¢

- OSUI[LA Urequnoul
UOATT 4R 390.10 JO 4SBO OPISPLVOy

---- aye AzeyO Jo pus JaMoy jo
OPIS JSOM TO PLOT JO ISOMTIION

SE eaneceic sens EO CON TO
qinos spor eq “Qimurms are
ARLE 8% ON JO WTOU “AF OT

Sma

CZ ‘ON JO YQIOU Spor CZ
pur ‘¢z ON JO W410 oT F 19AQ

"77" TZ ‘ON JO YQIOU sprVA OOT

“ALVIVOO'T

VAIOMLOUUBE |
|
|

VLOULQUUR(T
VIOULOUULG
2LOULOUUB(T

B1ourleuded

VLIOMLOU AVE

BIOULOTUG(T

vIOuUle TUR (Ty

PLOULI MUR (T

vLOTIOUUR(T

2LOULIUME (7

2 LOULBUTR (T

LOULOUTR(T

2LOULBTUB(T |

BIOTIOUUL(T

"dIHSN MOT,

tg

GS

9F

OUNTY.

1
J

CusHING—GErOLOGY OF CLINTON C

“OLOIYO

-ogfd oginb oy1déne fqsoiaz AOA |----°--> -oseqeiq |------->--- OP LUBY “WH of! 'N 4G | 76 ON JO YANO spavd Moy YW 777 YSanquel[a | 96
‘SSUUI-PUNOIS ot) ULopue;quioy
ueeIs 9[qeiepisuod {98j3s\1900U
-aqd asepooyz.1O ose, suoreumny |---> >>> OTMOISOM) sans vee es OPLUB.L “H o0L 'N SITES. |] OPP BOE *risiseicisissims cis S55 prox
| Ivou ‘s,10}SqaM JO JSOM SoplUT Z ysiuquella | &6
Baie siweinegring Sticisieie Tis aire sas test Sosa i+ OG CEC sr sae meee SSLOUN)) “WT oGh “S ‘WF GE | 77777 * BP CON JO YIN spavd OG |--- YSInQuoTTA | LF
: ‘ss1ous |
UI 9UOZ-IBEYS 10 BVYIp porvoys |
B Joqgio fomyonis onsvporyeg (a) Si CO Oe ss1omy “7 oCl °N SUNG 2 al || ae sk ere ee oe Opis JSve UO peor
-Aq ivou “6p ‘ON JO YQNOS ofim F > ysinquelTa | SP
"qsory ogi1nb
‘oUIAI[O pur redspyoy o1ytadqdiog |- oseqerp eulAl[Q ;-77> 77777777 SSTOU4) ‘N POON St altace meee site ot $1098 9 MA
ulody SoTIui Z ATIvoU ‘S49 MOH
“U1B3109 JOU STOMA} OIG sifqQ ogtsoddo ‘s,tegsqa Ay
ynq ‘atyeq Aq paqiiosep o10M WOIy YINOS pvor Jo opis yseqy - ySanquoelta | 6F
wey? JO OMT ‘oye, Avsnve |
-jeyy) reddy jo o10ys 380M OT}
WO WMOYS [TB 91B 29 04 GG SOMIG |-7-77 7 77> SOSBOCIG |bena wan “775 "* Sslomy TEC AUIS Senile os Aa, seek ce ees syd [ey ogis
-oddo Aj1voeu osnoy qnyjo B 4e
“SSRUI ‘99 Jo YQIOU 9oTRASIP & 9ZIMY |--- e1oOMOUUeG | 19
-punois UL opuatquroy ory dion A
-oIpt fegiuojdmvo suiqovorddy |- eseqevip eutat[g |*----- 77> >>> sSIOly) AEF (Od, INE || HG PH] SBE ose @9 ‘ON JO YQA0U spavd Og |--* VaotoUNEd | 99
‘orqtadydiog |-"-- -"-- -eseqeiq |---7-7*77 77" Ss1otly, “A 008 °S ‘ayg@ | c7777* FQ ON FO YQA0U spavs QZ |--~ VIoMTeUULd | 9
ST QMONT OSL sina saa as JORBCBIG els tae se se oe Sslouy) "HW oGL (N Qy@ |) 7777" Eg ‘ON JO YJLOU spavd GZ |--- VAoMIoUUBG | F9
‘19 ‘ON 03 repimig ‘otaAydiog |-------- -oseqeiq: |-7"7-"-"---- ssTouy “REGO ON || QUdEO) Whee | eSemcc 19 ‘ON JO yQaou spared Og |--- VaomMoTURT | ¢9
SESS PRP Se Th D IS OSLER ease SE ORO KOH (6 Pally oe “7 "> ssTomy oni SN 5 {te ane 19 ‘ON JO YQNOS spavd OZ ~ BIOWOUUB(T 69
SOVATUATT COG Illa a ase sek oseqviq |°-7-7- "777-> gsTomy “a Tape) Mine |] OSS 6¢ ‘ON JO qyA10u spared QOZ |" VaomleuUed | 9
‘6S “ON OF!] ony |---- 77-7 eseqriq |-7"77* SBR sslouyy "A c0S'N | “ULE “4F¥G | -77--> GE “ON JO YQuOos spared JT * vrourouued | 09
“peqliosop oe “APY OMG HOM
ulvgreoun st yy ‘oye, Avsure
-yeyQ eddy Jo o10ys ysoM O49
do UMOYS [[B We LQ OF GG SOMIC |------ “--eseqeiq |---"~" *777-> Sstomy Oa BN ONG | uae fe Miynsy || Cpa mCoc co ede o Solar - [oIOT]
qulog avIpuy ‘esnoy yroq yy |--~ vaomouurd™ | 6¢
“‘SMAVNGY “ANY N ‘STIVM “ANTULG “HLGI AY | *ALITVOO'T *dIHSNMOT, ‘ON
|

TATE GEOLOGIST.

RT OF THE S

O

Rep

*posodurooeq

“Fooy p POPTMRF ST

*pesoduroosep ATW SI

“‘qOoy MOJ V ULTPIIM 9OLMG poglnRT

“Gp JO Youraq vw ALQeqorg

o1ISnV
0} UOTJIPpL UI Ssvt-punois oy
UL Opue[quLoT, UMOIG pue 91}
-O1G eUIOS fOUTAITO 9[qRtopIsMog

“YSolf JON

*CTOATPOedsad SOTOUL MOF V puL
495 UF ZF JO sotouraq Inojz uy
p “Wpia

afqeiaea S10 JO soTouRAq fazts
adie, jo sivdsppoy od ydi0g

‘[eplopeps Aue
yeqaouos ‘iepluis ATOA o1v
991Y} GSUIPI—d.oONS 9} PUB SITLL,

: *poypury st
fozru0jdurvd o}lonBe OJUL sepeIy

‘SMUVWAY

ee ie poe “OSEQBICL

BS ieee ee osSVqeiqd

---- oy nbiqouoyy

BENS og1u0y dure dg

TR ae OSBC BIC

9 t asVq eid

“aSBGLIP OULAT[TO

-OSVqVIp OULATTO

~ OSBGCRIP VAIATTO

gredeniesl asUquiq
“INV N

Re ae, “yo SSTety)

ST le ee SSTOUX)

oe ae a A SSIOUX)

fe eee ee cae aes SSTOUK)

ae Awe el SSloU*)

---guogsourry AzeyO

---guojsoumly AzeyO

Fie, Oe Maas foe SSTOUNY)

Pg oak ot, SsTtouy)

a wad tate SsTour)

rhe s FAatae SSTOULY)

Rts Pa eo SSTOUX)

heise ~>>>> = SSTOUs)

“STTIV A

‘dH 009 “N

“H off “N

“HL 009 “N

“HL 088 “8S

“dH oST N

“AH 008 “N

“H o0L *S

“Hl oS9 N
mae
“H o0L “N

“H 008 (N

(4) “95 OT

“WP

WSs

“WT

“ur

“WS

“Wy

“WS

ie as vay yunoW

Jo oSpo ysvo jo yy1ou pros Kg

sosoon.c67 TL ‘ON JO ygnos oprur $

osnoly SLOW JO Yovqd spor Moy V

§,00qSMIO

‘arequnom A11ay, JO odols qION

“""* pp “ON OF SOTO

Spagna are esnoy
jo qynos efi F

s----s aL] Pu pvor u9IMyjoq

PIPy UL “Z “ON JO [Nos spor og

oyvy rou ‘Armenb

sAvq Jo YJnos pley ysuy uy

*O “d IBY Jo Jsomyynos opr F

“-""- ZOT ‘ON JO YQaou spied Cz

Haars 66 “ON JO YQat0u spared Cy

diswicds 86 ‘ON JO YysoU spavd QOT

Soe Se me 810008

“AY Ikou pror oyy 04 osolo

‘TE 989M JO Opis YZNos UG

“HLCT MA

*MLITVOO'T

2 ee nied
aia ula
eee ae niag
Nett ia uldd
Cae he ae ee uilog
eee. wel niod
aang spe ae nied
“-- Ysaunque,lpy
“-- YSinque[[q
--- YSanquelpy
“=> Yysinquel[y
“-* YSunquel[ a
“>> YSainq WET

“dIHSNMOT,

me)

cy

VV

~~
ao

ai

CusHina—GroLogy or Criinton County.

| |
Une eo | | | |
1 4seHre] oY} ‘SUOISTATP 9a1q} UT |* oseqeIp eULATTQ |-7777 7777777 sslouy “H 008 °N | =f Gig | aoe ore eee ae: YOO Ona,
| | | 19A0 9VOHOPLAG PAYA JO WSoM gous? OF
*pesoduiooeq |--------- SIAL. PPR FIs senses ssTauy G6 KAY INE |} Ce he |) SSeS ee Sf ON JO SOM Spavd OT 6e
‘OpITs 9qy |
ur ojopidea yout *{ posoduroseqd |----- So BOSe OCT Cilia meas ae oe ssToux) “WT of8 °N | SO OPE EE ree Sechsicla Peli yoorq ana,
IBAO VOPLIG ISA JO WoM opLuE ~ |--- >>> > OVUBIVG Re
‘posodimooep Ajqviepisuog |------ 777 OSU OUIGiall|p wea: alo sslouy "A of8 (N G11 So eee, OOS OS EA ea ees YOO.LG |
| ot} Aq ge “ON JO YQuOS spavdk QP |--7-7-7 oruBirg | ye
‘SOPITOLONUT YIM SSeps "i
Surmoys ‘padsoserid oie ssrous
oq} 07 OSOTO sqjuoUIseay ATWO |*-77- ((DV@EEMEGE |PSR S22 95345¢ SsTouy) ‘WH 008 °S (4) Wee OS Ieee SR COR MOr apIsSpvod |
}eya Aq ‘yooag AJ, 10A0
eDPIIG YSty JO ysvo spark QOT |*---7> -ovUuRARE 9¢
“UL | Leyyo |
eqs “Ul Z JO ouO ‘SUOISTAIP OMY, |--------- eseqeiq |--~--- 7-=--= §S1ouy) "TT 008 °N STC ue FE “ON JO YQNOS spavk Og |------- DvUBIBS | ce
cea ahs as Rtghp aba F ceajanmee Uphe RWe ss ilies SCSI SICGT |] SASSER = OSS OSes she i009) || “oT 008 “N "ul $¢@ | -----"- s[pVz YS oY 9Aogu
SPOL OF ‘IMAI oVUBIVEG OY AG |---7--- dBUBIEG tE
*qovquod SUOTR po Vlo0e1q |
SI ssteus ‘fpoesoduooep ony, |-----77-- OSEQBICL |-=> > a> *->> ssreuy "NT o0F “9 SQ ip phe ice oils exereisisteh= a releieaiaisho aia peor |
| JO YA10u ‘vissny Fo ysvo yeu |------- ovurieg | ¢¢
‘eqtorq |
ueeis = e[qelepIsuod suieyuog |------ SROMNTONSO Cis pass inans “77> sslouy ‘HA 008 “S rt) ey ee ea seisiela tere eS prag
DVUBAIBY IBOEU ‘BHUVI[IA DBUBIBS
‘oy1opvur JO ysvo pvor jo qqaom 4sug¢ |------- ovuring | Ze
ToOnwW fopuetqaioy ou ynq |
‘SI1QOIQ O[99I[ fUlOp[eS OUIAT[O |~~-~ ~~ e4yIyOInNOY |*ouoysomIy WOJUOTT, “a ‘UlG 95% | ~------- gulog Fug Jo II0u
gsuf oyey suore se1usodxe
; uozUeIy, Jo pue FNos pavmoy, |---ySangsyetq | F
‘pourrgqgo oq Avur [eIseyeUt
ysery ojinb fouraljo guepunqy |---- oyimbriqomoyy |-- ouojsomly AzeyD "A 008 'S SULT Gh Hl Fines rie ys cna oe ores mor, |
-BjS AVMTIVI QUIOg Yuj_ Jo
“qavde sp& Yjtou spark Ezy Gulog yurgq
G SUISVIOAL SUOISTATP J4S10 UL 0} YSngsyye[q wow pror Kg |---ySmmqsyriq | T
st {ssvul-punois 94 UL 94\901q .
pur apuerquzoy aMmorq orgd
-IOULOIPL fysoay puew omiatyqd
-iod ‘eqyiaojdurs surporoiddy |- esuqeip eutal[Q |----77 7777 7- ssieuy “H o0L "N (Gy PCn TT On Re SOC IC OCI TT ‘ON 90119817
| | JooyOg Jo oagued oy} ynoqy |-------->- nog | pz
“SMUVNAY ‘HHVN ° ‘ST1VM “UMIag “HLA A *“XLITVOO'T *dIHSNMO, ‘ON

Report or THE State GEOLOGIST.

|

‘opue[quioy wee1s
a[quiopisuoo pur oMeusvul

surejuog ‘100d o1njonds MOT |*

‘Oran OMIA aog |= --= == 95

*pesodmovep

qonm {<yoayoodsei ‘ur g pue
UL Z JO SoToUvAG [[VUs O4 SUPT |-~-> 77> -oseqeiq

‘poreeys

‘orqqes oiseq ynq ‘oxIp e@ JON
*posoduos0q
‘QUTATTO puV

eyrsux omudqdiod ‘poasuryo
-un SpTZavd SuUL9g DUTLATTLO

eqg uode ‘qsouy oginb ‘fyeorddy, | oseqeip OULAT[O

|
|
“SUUVINAY | “AWVN

tk Bie a Le SSTOU+)

Peres tk SSTOUL)

Seo ce yan es gt SSLOILY)

Fits) a aemre hee SSIlOUy)

Fo tate. & pie SSIOUY)

ee a ae ace SSO)

(4) “A 008 °S

“H 086 °S

BCI OG ScOn ap cr OT ‘ON 09 9S0[Q
ssicinis/eio\sismscvsieictsis\« VSPIIq PLOF
-poy jo pue yyNos Fo 4svo asne

“‘YJNOU sj LEU *YooIg plop Aq

aes = ee oe OF “ON JO ToOuvrq V

“UMOJUBUTY VO

oa a OBUBIBS

Deletes OBURLBS

Roe ea IBUBIBS

pe Seca rae OBUBIBS

LOT

90T

16

SP

If

STIVM

*XLITVOO'T

“dIHSNMOJ,

ON

a

Cusuinc—GroLocy or Crinron County. 527

Series VI. There has not been sufficient time at my command to
bestow on the Pleistocene deposits the attention they deserve. They are
widespread throughout the county, often in sufficient force to completely
obscure the underlying geology over considerable areas. They were, in part,
formed by glaciers and the streams to which they gave rise; in part, in the
body of standing water which occupied the Champlain valley just after the
retreat of the ice, and which had, at first, a level much above that of the
present lake, when it was probably fresh water, while later it was an arm of
the sea.

Glacial deposits. Away from the lake, the county is covered with a
heavy deposit of till. Over the high plain it is widely extended and largely
masks the irregularity of its pre-glacial surface. In the hilly tract it is mainly
confined to the valleys, though often prominent on the gentle northern slopes
of the ridges. Sections show it to be mostly very stony and very sandy, as
might be expected from the wide expanse of Potsdam country over which the
ice moved.

Moraines have been noted at various points, but any attempt at mapping
them would be premature. Much of the surface of the high plain is insuf-
ficiently drained, abounding in swamps, some of very large extent. Rough,
jagged boulders, mainly of Potsdam sandstone, are widespread over the
surface, often forming veritable trains, and being exceedingly numerous.
Some of these Potsdam boulder trains extend well into the gneiss country.

Glacial striae have been observed at many points. They are commonly —
well preserved on the palaeozoic rocks, but none have been noted on the older
rocks, although these are often well polished and smoothed. Along the lake
their direction is approximately that of its trend, those observed varying from
S. 15° E. to 8. 15° W. and those on the high plain have the same general
direction. As the hills are neared and entered, however, the general direction
is to the southwest, corresponding to the general trend of the ridges and
valleys.

A magnificent, long, esker-like ridge, which well merits description,*
occurs in the county. It is found in the low strip, only two or three miles
back from the lake, and forms a topographic feature of sufficient prominence
to be clearly brought out by the twenty-foot contours of the new maps. First
recognizable in Beekmantown township about two miles south of Ingraham
post office, it runs north in a curve to that point, then bears to the west

of north through Chazy. In the central part of that township its course is

*Mr. S. P. Baldwin has noted the presence of this ridge. American Geologist, March, 1894, p. 177.

or
bo

Report oF THE STaTE GEOLOGIST.

interrupted by a wide marsh; and by protruding ledges of rock, but after an
interval of a mile it again appears and runs north to the Chazy-Champlain
line, finally disappearing one-half mile beyond that line. It rises, in general,
about thirty feet above the ordinary level and the base has a width of a
quarter of a mile. Its surface is 120 feet above the level of lake Champlain.
It does not exhibit its entire mass, as its base is buried in Champlain clay.
Assuming that the disconnected portions are parts of a single ridge, as seems
highly probable, its entire length is ten miles. No good sections are exposed.
A three-foot cut in it, two and one-third miles southwest of Chazy village,
frequently shows somewhat rounded boulders mostly of Potsdam sandstone, a
few of which reached one foot in diameter, embedded in a matrix of coarse,
brown sand, No signs of stratification were visible, but the opening was not
a very recent one.

Champlain deposits. The term “ Champlain,” as here used, merely serves
to discriminate the deposits formed under water in the Champlain basin, from
those formed upon the land. During and after the retreat of the ice, the
glacial deposits on the low strip were covered by deposits laid down in the
marginal portions of the body of water that occupied the basin at that time,
the present lake beg its shrunken remnant. The mountain streams brought
down vast quantities of sand, building up large deltas at their mouths, and of
mud, which was deposited farther out and also along shore between the
deltas. As the water level fell from time to time, the sand deposits were
pushed farther out and formed at lower levels, covering up the clays of
the preceding stages. During much of this time the Champlain basin was
occupied by an arm of the sea, and the marie clays and sands are fossiliferous.
The fossils can be collected in abundance at several points in the county. The
sand delta deposits formed by the Saranac, Ausable, Little Ausable and
Salmon rivers are very widespread in the eastern part of the county. At the
higher levels they are confined to their respective valleys, but lower down
they become confluent. Much of the eastern portions of Ausable, Peru,
Schuyler Falls and Plattsburgh townships is covered by a wide, dreary
expanse of sand, often bare, sometimes with a sparse covering of coarse grass
with huckleberries and stunted pines, and which is dreary and monotonous in
the extreme. Dunes are quite frequent, especially where the sand has been
trenched by the present streams.

Some of the evidence collected mdicates that at first the water level
was at a greater altitude than has heretofore been recognized. Both in

the Saranac and Ausable valleys, the sands have been found to run up to -

CusHING

GEOLOGY OF CLINTON CounNTYy. 529

the height of 1,000 feet, and some of them are in such situations that they
‘an not possibly be regarded as river gravels and sands. This matter needs

further investigation.

METAMORPHISM OF THE Pre-CAmMBRIAN Rocks.

After the intrusion of the gabbro, and prior to the commencement of
Potsdam deposition, the region was subjected to intense dynamic meta-
morphism. The precise results produced would vary with the physical and
chemical properties of the rocks concerned, but, broadly speaking, they con-
sisted in the foliation of the rocks and the granulation of their contents, with or
without subsequent recrystallization. The gneisses were granulated and sub-
jected to a stretching process, by means of which the foliation and some,
at least, of the banding was produced; rocks like the gabbro dikes being
drawn out like the rest, and made to appear like an integral part of the series.
While some of the gneiss is characterized by a cataclastic structure, other
portions of it seem to have been completely recrystallized, and the different
minerals seem for the most part to have formed at the same time, few, if
any of them, showing idiomorphic boundaries against the rest. That this
recrystallization was not the final result of the metamorphism, is shown by
the ‘frequent pronounced undulatory extinction shown by the component
minerals of such rocks.

The anorthosites and gabbros were granulated and stretched in the same
manner as the gneisses, though apparently being more resistant to the latter
process. In the less feldspathic anorthosites, foliation was thus produced,
giving them their gneissoid aspect, and in them more or less recrystallization
took place with the formation of minerals foreign to the parent rock, by the
reactions of the various constituents on one another, much garnet, hornblende
and biotite thereby resulting. The stages of the process of granulation can
be studied to as great advantage in the Clinton county anorthosites as in
the Canadian examples so exhaustively described by Dr. F. D. Adams.

The basic gabbros seem to have been characterized originally by an
ophitic structure, but as a rule they are more thoroughly and finely granulated
than the anorthosites. They are often of such fine grain, and their boundaries
against the enclosing rocks are so sharp that the resemblance to dikes is very
striking. Reaction rims are a prominent feature in these rocks. They almost
always contain hypersthene, which is not common in the anorthosites and less

basic gabbros. In many cases the rock seems to have undergone complete
B4

530 Revporr of THE SvareE GEOLOGIST,

recrystallization, and when this is the case a considerable amount of
untwinned feldspar is present.

These basic gabbros vary in grain down to very finely granular varieties,
which are identical in character with the “shear-zone” rock from Avalanche
lake, described by Kemp.* A regular series can be made out from rocks
with ophitic structure down to these finely granular varieties. It seems to
the writer that these shear-zone rocks must have been originally of the basic,
ophitic type, and then they are often found in this much granulated condition
because less resistant than the massive anorthosites to the forces acting
on the rock. Where such bands are present they would represent lines of
weakness. But their different mineralogic composition is not regarded as
resulting from such action, but as largely a primary difference.

These gabbros may be regarded as basic segregations from the anortho-
site magma, or they may represent a period of igneous activity subsequent to
the anorthosites. They certainly have a much wider distribution. So far as
the writer is aware, data are lacking at present by means of which either of
these propositions may be demonstrated at the expense of the other. Later
observations by both Professor Kemp and the writer, clearly show that these
ophitic gabbros are younger than the anorthosites.

If the writer is correct in his belief that the diabases are of Pre-Cambrian
age, they must have followed the metamorphism of the rocks, as they are not
affected by it.

Post-Orpovician DtsturRBANCE.

After the deposition of the Palaeozoic rocks, came the period of the
Green mountain uplift in Vermont, and its effects were felt on the western
side of lake Champlain. Though but a comparatively few miles west of the
district in western Vermont characterized by sharp folds and thrust faults,
the effects shown here are apparently limited to normal faulting, accompanied
by a very trivial amount of folding. The dip of the Palaeozoic rocks is but
slight, seldom reaching ten degrees, and more commonly not over five degrees,
and is prevailingly to the north. Wigher dips do occur, but are invariably
local and in almost every observed instance can be demonstrated to be due to
proximity to a fault. Very low folds are often to be made out, but can
hardly be considered as constituting a prominent structural feature. Further-
more, there seems to be no system in their presence or arangement. They

trend and pitch in various directions. Faults however abound, ranging from

* American Journal of Science, Vol. XLIV., pp. 109-114.

PLATE IV

WYNKOOP HALLENBECK CRAWFORD.CO. .

ANORTHOSITE ON HALLECK’S HILL; SHOWING THE WELL GLACIATED SURFACE,

PLATE V

WYNKOOP HALLENBECK CRAWFORD GO...

NEARER VIEW OF THE SAME.

Lhe

<

ar ¢
y

Cc:

me ce Ne elf

aS
72

CusHING—GroLoGy oF Crinton Counry. 531

insignificant breaks, to great dislocations which have a throw of 2,000 feet,
and possibly more, and which can be traced for several miles. The possibility
of the presence of thrust faults has been constantly borne in mind, but the
evidence for their existence has not been forthcoming. In the majority of
cases the hade of the fault is not to be made out, but it 1s at least high. Some
can be demonstrated to be normal faults. By them the palaeozoic rocks are
chopped up into a series of small blocks, and they are so prevalent that
whenever the rocks are concealed much uncertainty necessarily prevails as to
what is beneath. It may, however, be laid down as a general proposition
that, in passing eastward from the Pre-Cambrian rocks toward the lake,
progressively younger rocks are met with. The exceptions to this in the
county are but few. The greater breaks have a northeast and southwest, or
a north and south trend, while the smaller ones range at some angle to these,
and so far as observed do not pass across them.

The Pre-Cambrian rocks have necessarily suffered also from the distur-
bances of this period, but in them the fractures are often difficult to locate,
nor is it possible to definitely distinguish them from possible earlier faults.
The topography often implies faults of great magnitude, but is wholly silent
as to their date. Kemp has written of the frequent faulting of the ore-beds.
Along contacts, too, decisive evidence of faulting is often forthcoming. ‘The
dikes are often faulted, the shift at the surface varying from a few inches only
up to the complete disappearance of the dike on one side of the break.
These faulted dikes give us the only evidence of faults which can, with
certainty, be ascribed to the later period.

Townsuipe Gronoey.
The more prominent features of the local geology in the various town-

ships will now be considered. The townships, in alphabetical order, are as
follows:

Altona,i7- ... . Page562. Dannemora, . . Page 535
pousalle tas! os 1% “545. Elienburgh, . .. 238
Beekmantown,. . iy (ON GaMGoersy =. Fis ioe Gino oe
Black Brook, . . Sto Ahiay erage 2+ wily” “ 549
Champlain,. . . 9 Seles) Blattsburghy ').:). feb58
@haziysiins ant tee Geo bo URSaTanae Ab si. | “5538

linuons ore tts “ 532 Schuyler Falls, . fC 42552

Reporr OF THE STATE GEOLOGIST.

or
oe
bo

linton.

The geology of this township is of no special interest. The Potsdam
sandstone is the surface rock throughout, and the exposures are few and
meagre. ‘The eastern half of the township is swampy and heavily wooded.
The central and western parts are higher and quite largely cleared of timber,

but are deeply covered with till.

Mooers.

In this township, also, the Potsdam is everywhere the surface rock, but
the exposures are better, more frequent, and somewhat more varied in char-
acter than in Clinton. Both townships form part of the high plaim which
slopes north from the Adirondack foot-hills. The dips are chiefly to the
northwest, but the presence of slight folds is indicated by the occasional ocecur-
rence of southeasterly dips. North of Mooers village occurs a series cf inter-
esting passage beds to the Calciferous, with a breadth of outcrop at the
Canada line of nearly three miles. They are cut off sharply on the west,
their place bemg taken by ordinary Potsdam, thus indicating a fault as they
dip to the northwest. They consist of rapidly alternating layers of white or
buff, well indurated sandstone, and dark bluish grey dolomites, which are often
sandy, the sandstones predominating. The dolomite layers, when forming the
surface, have a peculiar habit of weathering, which may also be frequently
observed in the dolomites of the Calciferous. Solution takes place rapidly
along two sets of planes, approximately at right angles, until the entire thick-
ness of the bed is eaten through (these dolomitic layers here have no great
thickness, seldom more than a foot), so that it is converted into a regular
series of disconnected blocks, of rounded outline, which project aboye the
meagre soil and present a yery curious and striking appearance.

If the Potsdam sandstone runs across the township without haying its
apparent thickness increased by faulting, the minimum thickness that can be
assigned to it is 1,500 feet, with the summit not reached, and the base not
even closely approached.

The township is quite heavily drift-covered. Along the streams in its
eastern half, considerable sand is exposed, but nothing at all comparable to
the great accumulations of the Saranac and the Ausable rivers. At Thorn’s
Corners, two miles west of Mooers village, the Great Chazy river shows
Potsdam sandstone in the stream bed, and over it on the bank an excellent
section, twenty-five feet in height, the upper ten feet consisting of coarse,

cross-bedded gravels, overlying a stony and rather sandy till.

CusHing—GroLocy oF Criintron County. 533

Ellenburgh.

Series I. The gneisses enter Ellenburgh from the south as three north-
easterly trending ridges. Ellenburgh mountain on the east, Panther mountain
in the centre, and on the west the less conspicuous ridge which forms San-
born’s hill and West hill. The ridges are separated by wide drift-filled
valleys, in which occasional rounded and glaciated knobs of gneiss protrude
above the surface. The Ellenburgh mountain gneiss, and that in the valley
to the west of it, is the ordinary red, microperthitic gneiss of the Adirondacks,

very acidic, poorly foliated, and cut by numerous veins of coarse pegmatit>

neiss Potsdam

and quartz. The pronounced red color of much of the rock is found to be
due to the infiltration of hematite between the grains and into the cleavage
cracks of the feldspar,

The gneiss of Panther mountain and West hill is highly acidie and much
of it looks like a red granite, and contains nothing besides microperthitic
orthoclase and quartz. In the more gneissoid exposures a monoclinic
pyroxene of strong green color creeps in. Very basic bands are not very
numerous and are, so far as observed, hornblende-plagioclase gneisses,

generally having this same green pyroxene in addition. The magnetite grains

534 Report oF THE STATE GEOLOGIST.

which occur in these gneisses are often surrounded by rims of titantite,
indicating that they are titaniferous, and this is frequently the case in these
gneisses throughout the whole region.

The facility with which gabbro grades into diorite has been shown by
several observers. These hornblende gneisses of the Adirondacks seem alsc
to grade into gabbro-gneisses whose igneous origin and relationship with the
greater gabbro masses are regarded as certain, and it is quite probable that the
hornblende-gneisses will prove to be merely a phase of them.

Series If and L/f are not known to occur in the township, though it is
quite likely that basic gabbros may be found in the gneisses.

Series [V. All the northeastern half of the township is oceupied by
the Potsdam sandstone, with prevailing dips of from 5° to 10° to the N. W.
The striking feature of the Ellenburgh Potsdam is its coarseness, even at
considerable distances from the gneiss, so that heavy conglomerates here
range through a thickness of 200 feet or more. A quarter of a mile west of
Star post office, and 200 yards south of the road, the Potsdam is found within
fifteen yards of the gneiss, a slight depression with no rocks exposed lying
between. The Potsdam is not as coarse as might be expected so close to the
contact, no coarser in fact than is the larger part of the formation in the town-
ship. This, together with the somewhat abnormal dip of the sandstone at
this place, gives rise to the suspicion of a north and south fault here (the
Potsdam hes to the east of the gneiss), and such a fault would explain the
sudden shoot to the north which the gneiss takes along this line.

In addition to the prevailing coarseness, much of the rock is very feld-
spathic, as is the case throughout the county in the basal Potsdam. The
less coarse, rapidly disintegrating, hematitic beds which frequently accompany
the conglomerates make, however, little show in this township. But there is
often a rapid alternation of coarse and finer beds, giving a thin-bedded
character to much of the coarse rock.

In the extreme northeast the conglomerates are left behind, and the rock
consists almost wholly of quartz sand. Yet even here certain horizons are
very pebbly. A very interesting exposure of the sort occurs in the bed of the
{nglish river at Ellenburgh depot. The dip here is slight and the surface of
a single layer is exposed over many square yards. The rock is a coarse, even-
grained grit but is set with numerous pebbles of white quartz, sometimes
over two inches in diameter. The horizon is well above the base and affords a
good instance of the coarse character which the rock holds throughout. In

addition to the quartz pebbles three larger rounded masses of sandstone, from

Cusutne—GroLoagy or Crrnron Counry. 535

four to six inches in diameter, were also observed embedded in the layer, as
well as two smaller pebbles of the same character. .

Series V. Of the eleven dikes found in the township only throe call
for any comment. Two miles from Webster’s mill, on the road west, an
enormous bostonite dike is exposed just north of the road. It is fully thirty
feet in width, has a dark reddish hue, and contains much porphyritic ortho-
clase, the crystals ranging up to one inch in length. Besides furnishing a
magnificent example of these dikes, it 1s also of interest for its indication of
the wide distribution of the bostonites. Just south of this dike, by the road-
side, is a dike of diabase (No. 96), two feet wide, which furnishes quite fresh
material, and is noteworthy for the strong pleochroism of its porphyritic
augite. One-fourth of a mile southwest of Star post office is a diabase dike
(No. 102), which furnishes the largest feldspar phenocrysts observed in any
diabase in the county. They are numerous, occur up to an inch in length,
breaking with lustrous cleavage faces which beautifully show the twinning
and complicated intergrowths of the crystals. The feldspar is close to
labradorite.

Series VI. The township hes beyond the reach of the Champlain
deposits. It has the usual heavy glacial deposits filling the valleys. A long,
massive, esker-like ridge forms a conspicuous feature near Ellenburgh depot.
It lies right athwart the valley of the English river and has saved the railroad
company the trouble of constructing a trestle, or embankment across the
valley. It has thrown the river out of its pre-glacial course and must have
dammed the valley for a brief time. The river has cut but a narrow trench
through it at its north end down to the level of the Potsdam in the stream
bed. The summit of the esker rises nearly to the level of the valley walls,
the valley being here quite wide and the sides of gentle slope. The length
of the esker is not known, but its width is fully one-quarter of a mile. No
good sections were seen, but a small cut at the base showed a coarse sand
matrix in which pebbles were set, these being somewhat rounded and _reach-

ing no great s1ze.

Dannemora.

This township has a more typical Adirondack character than any other
in the county, with the exception of Black Brook. The massive ridge of
Lyon mountain hes largely in it, though the summit is just over the border

in Saranac. The two largest lakes in the county, Chazy and Upper Chateau-

536 Reporr or tHe Srare GEoLoGIstT.

gay lakes, he, the former wholly, and the latter mainly, within its borders, and
the latter is, furthermore, a quite typical Adirondack lake.

Series I. The gneisses constitute the larger part of the township, the
massive ridge of Dannemora mountain occupying the eastern portion, Mount
Lyon in the centre, and the range of hills which extends into Ellenburgh as
Ellenburgh mountain on the west. Much of the gneiss is of the ordinary
acid, microperthitic variety, with the ever present bands of basic hornblende
gneiss. On Dannemora mountain, along with the red gneiss, is a white gneiss
streaked with black, which contains a quite pleochroic green monoclinic

pyroxene and much titanite. At Lyon mountain village, the ore-bearing

SL

Potsdam .

eneisses are also pyroxenic. They are well foliated, red gneisses, made up of
quartz, orthoclase, plagioclase, green pyroxene, deep orange titanite, a little
hornblende and magnetite. The pyroxene is strongly pleochroic, like that at
Dannemora, a being greenish-yellow, & and ¢ green. The presence of so much
titanite in the rocks enclosing the magnetite deposits is interesting. It never
appears as rims round the magnetite, as it does in some of the hornblende
onelsses.

Series II, Not present in the township so far as known.

Series ITI, A single small knoll of basic gabbro occurs nearly a mile
east of the lower end of Chazy lake, with gneiss in close proximity on the
west, and Potsdam on the east, while the gneiss of Dannemora mountain is
only two miles away eastward, so that this gabbro is undoubtedly to be
classed with the smaller masses which occur interbanded with the gneisses,
The rock is somewhat gneissoid, but readily identifiable in the field as gabbro.,
It is not completely granulated, but of the ophitic type, showing large

individuals of labradorite and nearly colorless monoclinic pyroxene of

Cusntnc—GroLocy oF Crinton County. 537

diallagic habit, both crammed full of intrusions. The interspaces are of
eranular structure, containing plagioclase and some unstriated feldspar,
neither with inclusions; augite, also without inclusions, hypersthene, horn-
blende, biotite and magnetite. This granular portion has evidently not
resulted from the mere granulation of the original rock, but is almost wholly
due to recrystallization. Reaction rims of biotite and hornblende around
magnetite are excellently shown. Garnet seems to be absent. Throughout
the county it is not so characteristic of the basic gabbros as of the
anorthosites, though frequently present in them. Aside from this exposure
no rocks of this series have been seen in the township.

Serves TV. A tongue of Potsdam sandstone runs into Dannemora,
occupying the depression between Dannemora and Ellenburgh mountains,
and traceable to Chazy lake, at the Chazy Lake House. Though hemmed in
between the gneisses, no coarse conglomerate has been seen, and most of the
rock is the red, hematitic, easily decomposing arkose. The best exposures
are in Steep Bank brook, two miles north of Dannemora village, and here
at an altitude of 1,500° feet, the greatest elevation known to be reached by
this rock in the county.

Series V. Forty-one dikes have been found in Dannemora township.
Kemp has noted eleven which cut the ore-body in the Chateaugay mine at
Lyon mountain, and five more have been described by Eakle from Upper
Chateaugay lake. The remainder have been found by the writer. Along the
west shore of Upper Chateaugay lake, and along the road north from
Dannemora over the mountain, are notable exhibitions of dikes. Four of
them are of bostonite, the rest are diabases. Only two of them need further
notice here.

Dike No. 46, west of the lower end of Chazy lake is of the bostonite
type, but abnormal. It is dark brown to black in color, non-porphyritic, and
rather coarse for this rock, with the trachytic structure not well marked. It
is almost wholly made up of rather large orthoclases, which are packed full of
inclusions of green hornblende and biotite. The two minerals have precisely
the same color, so that in many cases it is Impossible to distinguish them from
one another, but both are present. There are also some larger, irregularly
bounded green hornblendes which seem secondary after a nearly colorless
monoclinic pyroxene, two cores of which remain in the slide surrounded by
the hornblende, which is of the uralite type. It is a curious rock, and if
classed with the bostonites, must run very low in silica for that type. Just

what was its original condition, is not clear.

538 Report oF THE STATE GEOLOGIST.

Dike No. 66, from Upper Chateaugay lake, is a typical olivine diabase,
in which even the olivine is surprismgly fresh. The pyroxene is of
lilac color, with quite strong -pleochroism, a yellow, b and ¢ lilac. — Its
phenocrysts are full of inclusions and markedly zonal. In the ground-mass
is considerable brown hornblende and some biotite, so that the rock grades
toward the camptonites.

Series VI, The Chazy lake valley has some features which suggest a
fault valley, but the lake is held in place by heavy drift deposits at both ends.
There are also heavy drift deposits at the upper end of Upper Chateaugay
lake. Bradley pond is but a remnant of a somewhat larger body of water in
a wide valley where the drift is unusually heavy, and whose surface is strewn
with multitudinous loose blocks of Potsdam. Three miles north of the pond,
in Ellenburgh, a watershed is formed by an accumulation of hills of modified
drift, sand and gravel with surface blocks of Potsdam, which stretches across

the valley from side to side.

Saranac.

Series I, Except for the southeastern portion, known locally as
Hardscrabble, the entire township is occupied by the gneissic series. The
most accessible exposures are those found along the Saranac river, from
Saranac hollow westward, the most notable being the section in the gorge
below the High falls. Excellent and repeated exposures are also found
along True brook. The gneisses in the township are for the most part of the
ordinary red, microperthitic variety, with the usual variations im the amount
of ferro-magnesian silicates present, and also with the customary bands of
basic gneisses, both the hornblende gneisses and the gabbroic gneisses
occurring. Along the North Branch of the Saranac, from Petersburgh west-
ward to Cold brook, are microcline and plagioclase gneisses which closely
resemble those in Black Brook township already described.

Just east of Russia, north of the road, is a strip of brecciated gneiss,
like that described by Kemp from Hammondville and elsewhere in Essex
county,* the gneiss being in angular fragments of varying size cemented
together by a mixture of chloritic and other decomposition products. The
breccia has no great lateral extent and is cut by dike No. 33.

Along True brook, in Lot 35, just above the old mill dams, are scanty
exposures of the only rock at all resembling quartzite which has been seen

in the county. Unfortunately the exposures are isolated, no others haying

* Report of New York State Geologist for 1893, Vol. I., p. 456.

Cusuinc—GroLoay or Crirnron County. 539

been noted within half a mile to the east, while westward from this point the
valley expands, and all rocks are heavily buried in drift. Gneissic ridges are
within a mile both to the north and the south, but the rocks accompanying
the quartzites in the valley are nowhere exposed. Megascopically, much of
the rock is white and granular, with occasional small red garnets showing,
and, but for the latter, looking quite like some parts of the Potsdam. Other
portions are coarser, showing both quartz and orthoclase, the latter predom-
inating, and with an arrangement of the quartz in leaves, resembling, in that
respect, the Canadian rocks which Dr. Adams ¢éalls “leaf gneisses, ””*

Under the microscope, the rock is seen to be mainly composed of

microcline and quartz, with some orthoclase, a little plagioclase, and occa-

ees

Clayburgh. y
Tayburg i

Anorthosite

sional garnets, the whole with a rather finely granular structure. A few
larger individuals give the impression that the rock has been granulated,
but 1t 1s not certain. In one of the two slides made, are found occasional
individuals of a nearly colorless mineral, whose parallel extinction, high
interference colors, smal] axial angle, and positive character are indicative
of silimanite, though it is irregularly bounded and somewhat broken and
crushed. Its presence is of interest, as the mineral is quite characteristic
of certain schists closely associated with the limestones, and may perhaps
indicate the presence of the limestone series here concealed by the drift in
the valley.

* American Journal of Science, Vol. L., p. 62.

540 Report OF THE STATE GEOLOGIST.

Series ITI. At Petersburgh, showing well just north of the road, is
one of the largest of the basic gabbro bands that has been met with in the
county. Measured across the strike the exposure is fifty yards wide, and
the full width is not shown, but within a few yards distance, on both sides,
ordinary red gneiss comes in. A few yards south of the river at Petersburgh
bridge, is a smal] exposure of similar gabbro, and half way between Russia
and Redford, is another with red gneiss close at hand. On the True brook
road, just before reaching the fourth bridge (the road crosses the Brook
several times), is still another, which looks lke an enormous dike ten yards
wide, enclosed in the gneiss.

These four gabbros are all alike in mineralogic composition, being made
up of augite, hypersthene, hornblende, biotite, magnetite, plagioclase (some
untwinned) and apatite. Unlike most of the gabbro of the region, they
totally lack garnet. The gabbro south of the river at Petersburgh has the
ophitic structure, with the large characteristic feldspars and augites, which
always occur when that structure is preserved. The others are all granular,
and have suffered recrystallization ; that between Russia and Redford having
the very finely granular structure of the “shear-zone” rocks. The Peters-
burgh exposures are readily recognizable in the field as gabbros, while that
on True brook more resembles the hornblende gneisses.

Series IV. The Hardscrabble district, a rather elevated plain between
the Saranac and Salmon rivers, which les partly in southeastern Saranac,
is occupied by the Potsdam sandstone, but the heavy drift renders it impos-
sible to accurately map its southern, western and northern boundaries. The
exposures seldom show more than the upper surface. The rock is thin-bedded
for the most part, commonly buff, but with some red layers; is coarse and
gritty, but seldom pebbly, and most of it disintegrates quite rapidly, few
well indurated layers showing.

Series V. Thirteen dikes have been found in the township, most of
which are decomposed diabases. No, 41, just west of the third bridge over
True brook, is a typical olivine diabase, with large olivine and augite pheno-
erysts, the latter of a light rose color and shght pleochroism. The rock is
quite fresh, much of the olivine being perfectly sound.

No. 82 1s the only bostonite met with. It cuts the gneiss Just east of
Saranac village, and is a non-porphyritic, dark red rock, which contains a
considerable amount of green biotite and of magnetite.

Series VI. The sand deposits of the Saranac valley run up the river

to beyond Redford, and are very conspicuous at that point, where they have -

CusHING—GEOLOGY oF CLINTON CouNTY. 541

an altitude of about 1,000 feet. One mile southwest of Dannemora, at about
the same elevation, is a considerable accumulation of sand with streaks of
gravel, perched on the valiey side about 400 feet above the river, and sand
at about the same level shows at several points between. Both here and in
the Ausable valley, these delta deposits of the old lake seem to run higher

than heretofore recognized.

Black Brook.

This is the largest township in the county, and hes in the southwestern
corner, adjoining Franklin county on the west and Essex on the south. — Its
western half is wild, and much of it is quite imaccessible. The valleys are
wide with few exposures, and the ridges are difficult of access, forest clad,
and with their northern slopes heavily drift covered. Hence it is extremely
difficult to find outcrops in sufficient number to permit of accurate mapping.

Series I. With the exception of the extreme southwest, the entire
township is occupied by gneissic rocks which, for the present, must all be
classed together. There is comparatively little of the ordinary microperthitic
gneiss. Such is found on the northern border, and on Palmer hill at the
east. But even on Palmer hill and along the river at Ausable Forks there
is much microcline gneiss, and much of the gneiss contains abundant green
monoclinic pyroxene. This association of pyroxenic gneiss with the Palmer
hill magnetite deposits is of interest in view of the like association at Mine-
ville, as reported by Kemp.* The same also occurs at Lyon mountain. In
some of the Palmer hill gneisses there are titanite rims around the magnetites,
a curious circumstance considering their juxtaposition to the ore-bodies.
These gneisses are well shown along the railroad just east of Ausable Forks.
In these exposures is a sheared strip, three inches wide, in a coarse pegmatitic
band, which consists wholly of slickensided chloritic material. Just east of
the Forks is a heavy band of basic gneiss, which is hard and firm, and
contains, in addition to hornblende, plagioclase, biotite and magnetite, much
hypersthene but no monoclinic pyroxene. It is the only rock of the kind
seen in the county. The peculiar microcline gneisses, which haye been
described on a previous page, are widespread in the central part of the
township, and the ponderous east and west ridge known as Silver Lake
mountain, is wholly composed of them.

At Union Falls, the river drops twenty feet over gneiss and passes north

eastward in a gorge, exposing an excellent section in which the very variable

* Report New York State Geologist for 1°93, Tart I., p. 44!

542 Report oF THE Stare GEOLOGIST.

character of the gneiss, as exhibited in the township, is well shown. The
main “portion is a well foliated rock of microperthitic microcline and
orthoclase, with quartz and a variable, but mmonly considerable amount of
hornblende, biotite and magnetite. Much basic hornblende gneiss is
interbanded with it. A mile and a half a little east of north of the Falls, in
a field a few rods back from the road, is a considerable exposure of a brown
gneiss which contains an orthorhombic pyroxene of too slight pleochroism
and too weak double refraction for hypersthene, and which is probably

enstatite. It 1s the only occurrence of this mineral yet noted in the county.

Anerthosite.

za PX

FS

Loe
10

A short distance to the east is a well foliated microperthitic gneiss holding
numerous garnets, a mineral which, as a rule, is quite rare in the gneisses.
Gneiss is well exposed for several miles along the valley of Great Black
brook, the best exposures being at Black Brook village. This gneiss is, for
the most part, a well-foliated plagioclase gneiss, containing also orthoclase,
some quartz and a considerable amount of hornblende, biotite and magnetite.

The long ridge called Leggett mountain, which hes in the extreme south-
west and extends into Wilmington, Essex county, shows frequent exposures

of red and lilac-grey microcline gneiss at its northeastern extremity. Along

Cusutnc-——GroLoagy oF Cruinron County. 543

with these, is a small outcrop of basic gabbro of the type that occurs
interbanded with the gneisses. Exposures elsewhere on the ridge were very
ditticult of access and were not reached, but it was thought probable that the
whole was of gneiss. However, Professor Kemp reports gabbro from the
ridge just over the border in Wilmington, and the place where the gneiss
ceases and gives way to gabbro must be left for future determination.

Series IT. Not far from the Franklin line, in the valley between
Catamount and Leggett mountains through which Little Black brook
meanders, occur the only exposures of the limestone series which have been
found in the county. But three exposures were found, and the extent
eastward is uncertain, but the belt passes westward into Franklin county,
good exposures occurring around Franklin Falls.

About two miles east of the Franklin line, and lying close up against the
side of Catamount mountain, a massive limestone occurs in which a
considerable opening has been made and the rock burned for lime. The
limestone is coarsely crystallime and much of it quite pure, but other parts
contain much green pyroxene, sometimes in great bunches making up the
larger part of the rock, sometimes more evenly scattered through the mass.
In places graphite and phlogopite occur, but in no great quantity. Locally
there is considerable titanite, and there is one finely crystalline, narrow band
composed about equally of titanite, pyroxene and calcite. A few small,
slender green apatites were noted, but are not common. The breast in the
limestone is about twenty feet high and 150 feet long. Not far distant,
farther up the ridge, basic gabbro crops out.

By the roadside, some fifty rods south of the limestone, is a small outcrop
of a crumbling, rusty gneiss, consisting of a nearly colorless monoclinic
pyroxene and microperthitic orthoclase. In addition it contains some
sillimanite, titanite and magnetite, quite a little pyrite, and large scales of
graphite along the planes of foliation. Associated with it is a band of basic
hornblende-plagioclase gneiss. These gneisses are like those associated with
the limestone elsewhere and belong to this series. No other outcrop of such
gneiss has been seen in the county.

Series ITI. The massive, northeastwardly trending ridge of Catamount
mountain is composed of gabbro, and is probably a prolongation of the area
over the border which makes up the Whiteface mountain mass. The two are
separated by a wide, drift-filled depression which is probably occupied by the
limestone series. The Catamount ridge is suddenly cut off on the southwest,
at right angles to the trend ofj,the ridge, and presents in that direction a quite

544 Report oF THE STATE GEOLOGIST.

precipitous face which looks like a fault scarp. Such faces are characteristic
of most of the ridges of the county and produce the same impression on the
observer as do those of Essex county, which Kemp regards as of the block-
tilted type.

The Catamount gabbro is of the anorthosite variety, and so thoroughly
granulated that large cleavage faces are seldom visible in the hand specimen.
Hence the prevailing color is white, the ferro-magnesian silicates not being in
large amount and always concentrated along planes, so that the rock is quite
eneissoid. Garnet is present, but not so prominent as in much of the
anorthosite. The thin section shows monoclinic pyroxene, hornblende and
magnetite.

Not far above the limestone quarry, basic gabbro outcrops, but 1s_ so
poorly shown that it is impossible to ascertain its extent. It is composed of
augite, hypersthene, hornblende, biotite, garnet, magnetite and labradorite.
It seems to have been originally of the ophitic type as it contains some of the
diallage like augite, full of inclusions, which characterize that type. None of
the original idiomorphic feldspar remains, however, and most of the rock
seems to have undergone recrystallization. None of the minerals have
idiomorphic boundaries except the biotite, which does not appear as reaction
rims round the magnetite, but in thin plates distributed through the rock,
In fact there is no sign of reaction rims of any kind in the rock. In addition
to the above the same gabbroic gneisses are found interbanded with the other
gneisses of Series I that are found so commonly in the other townships.

Series LV. No Palaeozoic rocks are to be found in the township although
the Potsdam sandstone almost reaches it on the north and east.

Series V. Thirteen dikes have been noted in the township, all of which
are diabases. Three of the very narrow ones approach augite-camptonite by
the augite of the ground-mass becoming idiomorphic. Nos. 84 and 86 are
very typical diabases, furnishing quite fresh material.

Series VI. The higher level of the sand deposits of the Ausable river
runs up the river some distance above Ausable Forks, at that point rising
some little distance above the river level. Just west of the Forks on the road
to Black Brook an excellent section, twelve feet im height, 1s exposed, which

is. as follows, from the top downward :

Lb. Soil.
2. Coarse yellow sand with a few boulders,. . .,. 2 feet
3. Fine white sand with no: boulders, ..-. «92> 3)“

t. Stiff, blue, jointed clay, weathermg whitey... . 1 “

CusHinc—GroLocy or Ciinton Counry. 545
5. Sandy, laminated clay, somewhat undulating, . . © feet 9 inches.
6. Laminated, clayey sand, much folded and contorted, 1 foot.

Tt

Alternating thin bands of sand and clay with occasional rounded
boulders, to the base of the section, with a six-inch clay seam in its upper
part, which unites with the upper jointed clay, No. 4, at the west end of the
section, but one hundred feet away is three feet below it. At the east end
everything is cut off by the sudden downward dip of the upper yellow sand.
The white sand, No. 3, contains thin streaks of fine gravel and occasional
small clay nodules, and becomes very gravelly at the east end of the cut,

The whole seems clearly a shore deposit in standing water.

Ausable.

This is the smallest of the townships, and lies in the southeast, with the
Ausable river forming its southern boundary except at the extreme east,
where a narrow strip of low sandy land belonging to the modern delta of the
river is included in the county.

Series I. The gneisses cross the river into the county at Clintonville
and continue thence northeastward about half-way across the township, when
they are overlapped and indented by the Potsdam, their line of outerop
swerving to the west and then to the northwest. The wide gneissic hill in
the western part of the township is known as Arnold hill, and is
topographically an extension of Palmer hill in Black Brook. The Little
Ausable river cuts through it in a narrow, steep-sided valley, apparently due
to a fault, with the gneiss showing grandly on the east side. At Clintonville
and northeastward from it, are also excellent exposures. Then follows a drift
filled depression a mile in width, beyond which the gneiss again crops out in
two low hills, round which the gabbro sweeps in a semi-circle.

The exposures are, for the most part, of ordinary microperthitic gneiss,
with some plagioclase gneiss toward the north, and with the usual bands of
hornblende gneiss. On Arnold hill are important ore-bodies. About one
mile southwest of Harkness station and near the railroad, is a strip of no great
width which resembles a dike and is probably a sheared strip. It is a finely
granular black rock, made up of plagioclase, orthoclase, hornblende, biotite
and magnetite, hence with the mineralogy of the hornblende gneisses.

Series ITI, Lying east of the gneisses, and forming the rather low

elevation known as Halleck’s hill, is an area of anorthosite. It has a breadth
30)

546 REPORT OF THE STATE GEOLOGIST.

of one mile and a half where it crosses the river from Chesterfield, and
gradually decreases in width going north till the last of it runs under cover
two miles north of Keeseville.

The district furnishes the most typical anorthosite to be found in the
county. While the rock is much granulated, some of it wholly so, there is
still much of it that shows partially unbroken crystals of labradorite that
reach, on occasion, a very considerable size, being found up to three inches in
length. A considerable part of the rock is almost wholly feldspathic, the
ferro-magnesian minerals occurring only in very small amount. The less
feldspathic portions of the rock are the most completely granulated, and have

a prevailing gneissic habit. In these varieties garnet is very abundant, often

o% aXe
‘>
Ss

BG REE SSS

Gneiss Anorthosite Potsdam

imparting a reddish tint to the rock. In them reaction rims are also a feature,
and a considerable amount of recrystallization has taken place. Openings
have been made in the more feldspathic portions of the rock in the vicinity of
Keeseville, and some of it put on the market under the name of “ Keeseville
granite.” It makes a very handsome stone, the large, blue-grey labradorite
crystals surrounded by a lighter colored granulated zone giving a very pretty
effect ; but no tests of its crushing strength have been made, so far as the
writer is aware. It seems quite resistant to weathering.

In several places in this anorthosite area are found bands of basic
gabbro, When finely granular, as is commonly the case with the thinner

bands, they look like dikes. The larger masses are often less changed and

CusHinc—GroLogy oF Crinton County. 547

show the rude ophitic structure already described. The larger feldspars often
broken but

frequently bent. In one slide is a_ well-twinned crystal, about seven

show beautiful pressure effects, the crystals not only being
millimetres long, in which the gradual variation in extinction from one end of
the crystal to the other amounts to 25°, showing a bending to that amount,
yet with no apparent breakage of the crystal.

The contacts between these basic bands and the anorthosite are often as
sharp and clear as intrusive contacts, so that slides may readily be prepared
consisting half of one and half of the other.

As has been already stated, these basic gabbros are so absolutely like the
basic gabbroic bands found in the gneisses, that there can be no question as
to the identity of the two. Neither in the hand specimen nor in thin section
can they be distinguished from each other. Both the granular and the
ophitic phases occur in both situations. It would seem most probable that
they are to be regarded as basic segregations from the main anorthosite
intrusion, which have been stretched out into bands parallel with the foliation
of the enclosing rock as a result of dynamic metamorphism. Such
segregation would take place mostly toward the periphery of the mass, and
such portions as were squeezed out into cracks in the enclosing rocks would
be mainly of this type. But on the other hand the frequent sharp boundaries
between the basic gabbro and the anorthosite, with no sign of gradation into
each other, and the much wider distribution of the gabbro, can not but give
rise to the suspicion that, at least in part, the gabbro intrusion may have been
subsequent to that of the anorthosite.*

A massive band of basic gabbro which is found in the anorthosite at a
point a little over a mile west of Keeseyille, just north of the river road, is
interesting as showing a gradation toward diorite. Monoclinic pyroxene and
garnet are found in the rock but are very subordinate to the hornblende,
which shows great development, while hypersthene is absent. A hint of this
is given in the appearance of the rock, which is more schistose than the
normal gabbro. The main interest attaching to the occurrence is from its
possible bearing on the origin of the hornblende gneisses of the gneiss series,
which the rock much resembles.

Two miles west of Keeseville, on the river bank, is a knob of gabbro
which is interesting as indicating a transition to gneiss. It is of brown color,

finely granular, and contains quite a little quartz and microperthitic

*Later work by both Professor Kemp and the writer demonstrates that much, if not all of the basic gabbro is of later date
than the anorthosite, as indicated here at Keeseville.

548 Report oF THE STATE GEOLOGIST.

orthoclase in addition to the ordinary gabbro minerals, plagioclase,
hornblende, augite, garnet and apatite. It 1s the most westerly of the gabbro
outcrops, but two miles of barren ground intervene between it and the
Clintonville gneisses.

Series IV. The only Palaeozoic rocks exposed in the township are of
Potsdam sandstone. The magnificent exhibition of this rock in the Ausable
chasm has been mentioned by many observers, and has been carefully
measured by Mr. Walcott.* Except for this river section, all the Potsdam
in the eastern part of the township is deeply buried by sand. The rock
exposed at Keeseville and in the chasm is quite homogeneous, of white, grey
or yellow brown color, and the fossils indicate that it is the upper portion
of the formation that is here shown. This, together with the lack of red beds
and conglomerates as the gabbro is approached, gives rise to the suspicion of
a fault contact. It is about on a line, also, with a fault which runs through
Peru and Plattsburgh, close to the lake shore.

A very interesting exposure of Potsdam on the west side of the supposed
fault is worthy of description. The locality is not quite a mile west of
Keeseville, not far west of the race track, and a few hundred yards southeast
ot School No. 5. Nestling in an indentation in the eastern face of the gabbro,
is a small mass of peculiar, very coarse conglomerate, capped by very red,
thin-bedded layers of feldspathic sandstone of the ordinary basal type.
The conglomerate carries very numerous, well-rounded quartz pebbles of a
reddish lilac tint, ranging in size up to two inches in diameter. With
these are occasional smaller fragments of orthoclase and afew dark colored
pebbles of decomposed rock, apparently of diabase. In streaks magnetite is
present in very large quantity, in well rounded grains. The coarsely granular
matrix looks black when fresh, but on weathering becomes mottled with
blotches of green chloritic material, which gives the predominant color to the
rock. In thin section, grains of quartz, microperthitic orthoclase, magnetite,
titanite and microcline, named in order of abundance, are seen to constitute
the matrix, and are set in a green chloritic-like cement, whose exact nature
is not clear. The coarseness of the conglomerate is astonishing when we
remember that it is composed entirely of gneissic debris, yet is in contact with
anorthosite, the nearest exposures of gneiss being one mile and a half away.

In the northern and western parts of the township considerable Potsdam

is exposed. It is, for the most part, a hard, flinty sandstone of buff color,

* Bulletin 81, United States Geological Survey, pp. 343-344. The boss of granite mentioned by Mr. Walcott, on the river
bank above Keegeyille, is of gabbro.

CusHING—GEOLOGY oF CLINTON CouNTY. 549

though on the north flank of Arnold hill, in the vicinity of the gneiss, coarse
conglomerates occur. In the central part of the town it runs down in a
curious way between two gneiss ridges. There is here a drift-filled valley, a
mile or more in width, which runs clear across the township, and was
apparently the track of a pre-glacial stream. Along the Ausable it intervenes
between the Clintonville gneiss and the gabbro to the eastward, but further
north, gneiss ridges form both walls. At the north end, the Potsdam-gneiss
contact is found near Mr. Harkness’s house. The well on the premises, close
by the house, penetrated hornblende gneiss at a depth of a few feet, while
only five rods to the northwest, flinty Potsdam was reached in a cistern. One
mile and a half to the southward, are two old openings in Potsdam sandstone,
known as Mace’s quarry. The rock is ordinary hard, massive, buff sandstone.
Less than a mile away on each side, are massive gneiss ridges, and we have
here apparently a pre-Potsdam as well as a pre-glacial valley. It is unfor-
tunate that the drift covering does not permit us to determine how far up
this valley the Potsdam runs, but there seems no reason why it may not run
clear to the Ausable river. It recalls the patches of Potsdam described by
Kemp from Essex county.*

Series VI, The northern slopes of Arnold hill are covered with till,
and the surface is plentifully besprinkled with boulders. The till covering
ranges throughout the gneissic area, but elsewhere in the township every-
thing of the sort is hidden from sight beneath the universal mantle of sand.
This surrounds Halleck hill on the east and north, running clear to the lake
shore and well into Peru. It extends up the Ausable valley beyond the
limits of the township, and at Clintonville and New Sweden is heavily banked
up against the gneisses, is bare and much drifted about by the winds. It
also extends throughout the yalley of the Little Ausable, even in its narrow
upper reaches, great drifts of it lying around and against the protruding

bosses of gneiss.

Peru.

The western third of Peru township is hilly, and occupied by the
eneisses. A plain of till, with a breadth of one mile and a half, borders the
hills on the east. Then there is a drop of fifty to one hundred feet, to the
level of a sand plain, which has a breadth of from three to four miles. For

the last three miles to the lake, rock ledges protrude frequently through the

* Report of New York State Geologist for 1893, Vol. I., pp. 454-458.

550 Report or THe Srare Groroatsr.
Champlain clays and sands, but from thence westward to the hills everything
is concealed by the drift and sand.

Series I. Three northeasterly trending gneissic ridges rise in the western -
third of the township. The most northerly of these is a narrow ridge known
as Burnt hill, which rises rather abruptly from the Salmon river valley, but
whose summit is only a little above the level of a plain of Potsdam sandstone,
which overlaps it on the north. In the central-west is the wide, massive
ridge of Terry mountain, and to the south is a somewhat disconnected ridge
coming in from Black Brook, the most easterly summit of which is called
Mt. Etna. The larger part of the gneiss is of the ordinary microperthitic
variety. A quite prominent gneiss on Mt. Etna is a quartz plagioclase gneiss,

with some microcline and orthoclase, and with hornblende, biotite and magne-

Gneiss

tite present in considerable amount, so that the rock is well foliated. The
Burnt hill gneiss contains much microcline, that mineral often constituting
more than fifty per cent. of the rock.

Series IT and ITT do not appear in the township.

Series IV. Potsdam sandstone. Though the Potsdam must occupy
much of the central part of the township, the exposures, with one exception,
are close to the gneiss, poor, and possess no special interest. At Lapham’s
mills the Little Ausable is in a new channel, and about thirty feet of Potsdam
is there exposed, all rather coarse, some of it red, but mostly buff or brown
in color. The dip is to the southwest, and rocks of Calciferous age surround
it on all sides. That in the river bed at Peru, one mile to the southwest, has
the same dip, while the exposures to the north and east dip to the north-
east, and a fault must lie between them and the Potsdam, this fault being

probably along the summit of a low fold.

CusHinc—GeroLocy or Curnron Counry. ddI

Caleiferous sandrock. Rocks of Calciferous age apparently form the
surface over most of the eastern third of the township, although no certainty
can be reached upon this point, due to the scarcity of exposures. The out-
crops are small and isolated, and generally give no clew to their horizon in
the Calciferous, being for the most part of the iron-grey dolomite which consti-
tutes such a large part of the formation. Just north of Lapham’s, are meagre
outcrops of very sandy dolomites, which weather to deep ferruginous, sandy,
brown crusts, and seem to belong to Division D, of Brainard and Seely.

Along the lake shore, both north and south of Valcour, rocks of this age
outcrop for a distance of a mile or more. The major part of the rock is a
hard grey dolomite, full of seams and balls of calcite, and in some layers quite
fossiliferous. Interstratified with them are thin bands of limestone, more
abundant toward the top. Here limestone is also found in irregular lenses,
which are full of fragmentary fossils, looking as if they had been worn on a
beach. An Ophileta-ke form also occurs, and is the only species found
entire. The rocks le in a series of low east and west folds, with a slight
fall of the whole toward the north. They are well toward the top of the
Calciferous, and are followed a short distance to the north, apparently
conformably, by the lower Chazy. The whole mass is penetrated by irregular
slaty seams.

* Chazy limestone. From Valcour northward along the lake shore, rocks
of Chazy age outcrop in a belt about half a mile wide, abruptly terminating
on the west along a fault line, the Bluff Point fault. The exposures are
rather infrequent, and the district needs detailed study, but everything seen
seems referable to the lower part of Division A, of the Chazy. On Mr. Day’s
land two quarries have been opened in the rock, one near his house and one
by the lake. In the upper quarry especially, the rock is quite fossiliferous,
and good collections can be made. A large Nauti/us is conspicuous among
the fossils. Mr. Day has an excellent Zetuites obtained from the quarry.
Trilobite fragments abound, mainly of J//@nus and Harpes, and several
species of brachiopods are present, Orthis costalis being the most common
form, ‘The locality is one of considerable palaeontologic interest.

Series V. Hight dikes have been found in Peru, of which six are
diabases, and call for no special mention. The other two cut the Chazy lime-
stone, near the lake shore, and are of interest on account of the rarity of dikes
in the county outside of the pre-Cambrian rocks.

No. 2, in the field just south of the Day quarry, is a typical camptonite,

the only one so far found in the county. It may be traced clear to the lake

552 Report oF THE STATE GEOLOGIST.

shore, a distance of some 600 yards. Unfortunately it does not furnish very
fresh material.

No. 8 lies one-fourth of a mile south of the other, and is a beautiful
mouchiquite. Material may be obtained in which even the olivine is quite
fresh. The strike of this dike would carry it over to the southern part of
Valcour Island, and it may be the same dike as the one found there by
Brainard and Seely. As far as can be told from the description, the two
are quite similar. But in so disturbed a region such identifications are

extremely hazardous.

Schuyler Falls.

There is little of interest in the geology of this township. The extreme
eastern edge of the Burnt hill gneiss comes into the southwestern corner
from Peru. With this exception the only rock exposed in the township is
the Potsdam sandstone, though it is reasonably certain that the Caiciferous is
also present in the east, obscured by the heavy sand. The western part of
the township is occupied by Potsdam, lying at a tolerably high level, and
continuous on the west with the Hardscrabble Potsdam in Saranac. The
gorge of the Saranac river, at Cadyville, is cut in the eastern edge of this
plateau, and exposes an excellent section. The old channel of the river lies
to the northward and is filled to the brim with drift. Along the Salmon
river the rock is well exposed at Schuyler Falls village, and less well at
Norrisville. In the exposures is much red rock, and some that is tolerably
coarse, but whether low or high up in the formation does not appear.

Series VI. All the eastern half of the township is heavily covered with
sand, the level ranging from 300 to 4Q0 feet altitude. Occasional cuts show
the clay below. Further to the west the prevailing cover is still sand, though
at higher level, and becoming more and more confined to the vicinity of the
river. Along the Chateaugay railroad the sand shows grandly, much of it
being bare and forming dune-like ridges. Cuts in the river bank at Morrison.
ville show an esker-like deposit of coarse sand and gravel, with small some-
what rounded boulders. Its summit lacks a few feet of reaching the level of
the sand plain, so-that its presence would be unsuspected were it not for the
river channel.* A precisely similar section is shown along the Salmon river
just west of Schuyler Falls, which may represent a prolongation of the

same deposit.

* This esker (7) is noted by Mr. Baldwinin American Geologist, March, 1894, page 177.

GEOLOGY oF CrLInron Counry. 5b

CuSHING

Plattsburgh.

No pre-Cambrian rocks occur in Plattsburgh.

Series IV. Potsdam sandstone. Except for the river exposures at
Cadyville just alluded to, the Potsdam does not outcrop in the township. In
fact, with this exception there is not an outcrop of any kind in the western
three-fourths of Plattsburgh. This wide belt must be underlaid in part by
rocks of Potsdam, in part by those of Calciferous age; but where the
boundary between them may lie is purely a matter of assumption.

Calciferous sandrock. By the Salmon river, at the bridge two miles

above the mouth, several ledges of a hard, dark blue, somewhat calcareous

eva
unas

dolomite are exposed. By the road south of the river a erey dolomite, with
seams and spheroids of calcite, is shown. Though no fossils were found, the
lithology of these outerops puts them in the Calciferous, probably well
toward the top.

At the pulp mill on the Saranac, three and one-half miles southwest of

Plattsburgh, the river is out of its old channel for a short distance, and
exposes a vertical section of some fifty feet, showing heavy, dark blue-grey
dolomites, which hold spheroids of calcite, and weather to a yellow color,

interstratified with dark calcarous slates. No fossils were found, and no other

554 Report oF THE Strate GEOLOGIsT.

exposures are near, to aid in determining the horizon, which is regarded as
Calciferous, though with some hesitation, it being possible that the rock
belongs at the base of the Chazy.

Along the road to Beekmantown Corners, north of Plattsburgh, a long
ridge of rock of Calciferous age is exposed, mainly of a flinty, grey dolomite in
massive beds lying nearly horizontal. In the bed of Kennon brook, nearly
to the Beekmantown line is a considerable exposure, exhibiting some twenty
feet of rock, the lower part consisting of dark blue, sparkling dolomites
mingled with lighter colored, more sandy beds and thin layers of white, hard
sandstone, while above are massive iron-grey dolomites. These beds are well
down in the Calciferous, higher layers coming in above them in Beekmantown.

Chazy limestone. The Chazy is excellently exposed on, and southward
from Bluff Point, and also north of Plattsburgh, where it hes just to the east
of the Caleiferous exposures described above.

Brainard and Seeley have written briefly of the Bluff Point exposures.*
The point is a conspicuous topographic feature, rising sharply to an altitude
of 170 feet above the lake, and being the only high ground along the shore in
the entire county. It is a fault block with a resistant stratum at its summit.
Nearly the whole of the middle Chazy and about one hundred feet of the
lower division are well exposed. By following along the ridge southward
from the point, into Peru, nearly the whole lower division may be brought
into the section. The whole series is characteristically fossiliferous. Along
the lake shore at the boat landing, the beds shown aré well up in the
Maclurea division, are much jomted, and contain abundantly a_ large
strophomenoid form, much like 7. a/ternata, of the Trenton, for which it was
taken until the discovery of Maclurea threw doubt upon the identification.
Several other species may also be collected there.

Just south of Bluff Point is a large quarry, worked in a layer of the
lower division in which the crinoidal fragments have a red color. Much
stone has been, and is being taken out, which, when polished, makes a

beautiful and striking marble.

The Chazy north of Plattsburgh is in a much faulted district, and has

been mapped in detail. At the normal school, beds of lower Chazy age are

exposed, which crop out again going north, and are then succeeded, just

(Op
oO
beyond the race track, by the lower Maclurea beds. These continue along the
road for a distance of nearly a mile, with a sinuous strike. They consist

mainly of massive, nearly black limestones, and are largely quarried. With

3ulletin Geological Society of America, Vol. II., p. 295.

Cusninc—GroLocy or Crinton County. 555

these are thin-bedded, rather shaly bands, with an abundant brachiopod
fauna. Just beyond the three corners, a little over a mile north of Platts-
burgh, is an east and west fault, bringing up again the upper beds of the
lower division on the north side. This is followed at once by the Maclurea
beds again, and thence northward the entire Maclurea division and a large
part of the upper Chazy appear within the space of a mile, the latter well
exposed and abundantly fossiliferous. The final exposures are less than half
a mile from the Beekmantown line, and are succeeded, in the direction of dip,
just across that line by massive dolomites of Calciferous age. If the section of
the Chazy here be combined with the Bluff Point section, a nearly complete
exhibit of that formation is obtained.

Trenton limestone. The best exposures of the Trenton to be found in
the county are in this township, but the base, the Black River limestone, is
nowhere exposed. Along the lake shore, just south of Bluff Point, and
extending for a third of a mile, are beds of Trenton age. They are separated
from the Bluff Point Chazy by an east and west fault, with a throw to the
north of about 200 feet. A small stream occupies the fault line. The section
exposes some 100 feet of the Trenton. At the south end the dip is steep, the
beds being tipped up along the fault. The rock is, for the most part, a black
slaty limestone with lighter colored limestone bands toward the base, which
contain the brachiopod fauna characterizing the lower 100 feet of the
Trenton in Chazy township. The upper two-thirds of the section is quite
barren of fossils, occasional trilobite fragments occurring. Similar beds
are found in the same position on Crab island, which lies one mile to
the eastward. The section there has already been briefly described. The
island is structurally a low anticlinal fold, pitching to the north about five
degrees. The upper 100 feet of rock exposed there, carrying a lamellibranch
fauna, is shown nowhere else in the county.

On Cumberland head, and thence northward into Beekmantown, are the
slaty exposures already described. They are younger than any of the Crab
island Trenton, and separated from that by an unknown vertical interval.
Just south of the breakwater at Plattsburgh, similar slates are exposed on the
shore, in which no fossils have been found, but in which thorough search
should be made, as they may be found to partially fill this gap. Litho-
logically they resemble the Cumberland head series much more than they
do the ordinary Trenton.

Faults in Series IV. The whole Palaeozoic series is greatly faulted.
Though much remains to be done in working out the faults, especially the

556 Report oF THE SraTe GEOLOGIST.

minor ones, the greater breaks stand out prominently, and deserve mention.
The Bluff Point Chazy is cut off sharply on the west by a north and south

ses
ae

Dx
WP
SaaS

[-Z

q

fault of considerable extent and magnitude. In southern Plattsburgh,
however, no rock shows to the west of the fault line. It may be traced to ~

Cusning—GroLocy or Crinton County. 557
the south into Peru, and well to the north also. We may call it the “ Platts-
burgh fault.” Just north of Bluff Point, the east and west fault, already
described, runs out to meet it. The throw of this, which may be called the
“Bluff Point fault,” is to the north, and an approximation to its amount may
be had. The entire upper division of the Chazy, 200 feet thick on Valcour
island, fifty to 100 feet of the middle division, and fifty to 150 feet of the
Trenton are missing, so that the vertical displacement is from 300 to 400 feet.
North of this fault, the Plattsburgh fault is not traceable for nearly four
miles, on account of the total lack of exposures, but north of Plattsburgh
city, on the prolongation of the fault line, is a displacement which is thought
to be the same. Here the Chazy exposures on the west side are sharply cut
off at an angle with their strike. To the east no rock is exposed for a
distance of one mile and a half, when the Cumberland head slates come in.
Though the fault line is strongly marked wherever shown, no data are
available for determining the amount of displacement. The throw is to the
east, and must be large.

Three-fourths of a mile to the west is another great fault, very well
shown, which brings up the Calciferous against the Chazy. The horizon in
the Calciferous has not been determined, but is apparently well down, so that
the entire lower division of the Chazy, over 300 feet thick, and probably a
much greater amount of the Calciferous, are faulted- out, the throw again
being to the east. This fault may be named the “ Beekmantown fault.”
It has a more easterly trend than the Plattsburgh fault, so that the two
appear to effect a junction on the Beekmantown line, shutting out the Chazy
altogether, and bringing the Calciferous and Cumberland head series into
contact in southern Beekmantown. The displacement here, therefore, must
be very great, as the entire Chazy, all the ordinary Trenton, and an unknown
amount of the Calciferous are missing, and 1,500 feet would be a very
moderate estimate of its amount.

These three, together with the cross-fault in the Chazy beds between the
Plattsburgh and Beekmantown faults, are the main faults in the township.
Small faults occur on Cumberland head, and the slaty cleavage there
developed in the whole series would probably be represented by a con-
siderable fault, were the beds more ngid. No doubt other faults occur,
but the paucity of outcrops renders their discovery and decipherment nearly
impossible.

Series V. Only two dikes have been found in the township, but they

are of interest as, together with the South Hero dikes described by Kemp,

558 Report OF THE STATE GEOLOGIST.

they are the most northerly of the post-Utica basic dikes known along the
lake Champlain meridian.

Dike No. 1 is exposed by the roadside on the road south from Platts-
burgh, a few yards beyond the point where it rises from the sand plain on to
the Bluff Point limestone exposures. It is a quite typical monchiquite, with
very abundant olivine phenocrysts, often perfectly fresh, which speck the
dense black rock with white spots. Occasional small porphyritie augites
also occur. The dike being so narrow, the ground-mass is very dense
throughout, and consists of small, slender augites, magnetite and _ sparse
brown hornblendes set in an apparent glassy base, most, if not all of which
has a very weak double refraction, and thorough investigation may show the
presence of analcite.

Dike No. 4 cuts the Trenton north of Bluff Point, and is near the south
end of the section. It is largely made up of a nearly colorless augite, which
occurs in two generations, phenocrysts, however, being only occasional.
Olivine is present, but rare, and can not be regarded as an essential
constituent. Hornblende is absent except for a few green, uralitic crystals
of secondary origin. Magnetite is present in considerable amount, and
there is also a notable quantity of biotite in the ground-mass, some, of
which is certainly primary. The rock contains numerous round white spots,
giving it an amygdaloidal appearance. In the centre of the dike is a strip
six inches wide which is clearly marked off from the rest, runs the whole
length of the dike, and gives the impression of a second dike cutting the first.
The rock is of the same character, however, though the white spots are less
abundant than in the main dike. Under the microscope these white
spheroids are seen to be formed of a colorless, isotropic mineral, which by
means of a gypsum plate, is seen to be optically anomalous, in that it shows
faint double refraction. The mineral seems to be analcite. Some of the
spheroids contain also calcite crystals. Inclusions of biotite, apatite and
hornblende, of rather large size, occur in the analcite. The spheroids are not
sharply bounded, but grade into the rock. Considerable analcite is also
present in the ground-mass of the rock.*

Dike No. 19, from Crab island, is quite similar. It is made up of augite,
biotite and magnetite, with glassy base, but it lacks the analcite spheroids, and
instead is amygdaloidal, the cavities being filled with calcite and zeolites

other than analcite. It has numerous and large porphyritic augites.

* Since the above was transmitted for publication, the article published by Professor L. V. Pirsson ‘‘ On the Monchiquite or
Analcite Group of Igneous Rocks” has appeared (Journal of Geology, Vol IV., p. 679). Pirsson shows the presence of analcite
to be a feature of these rocks. The analcite in Dike No. 4 seems to be primary.

GroLogy or Crinton Counry. 559

YUSHING

Series VI. ‘The widespread sand deposits of the Saranac, form here, as
in Schuyler Falls, the most conspicuous feature of the Pleistocene deposits.
Away from the river in the northwestern part of the town, heavy morainic

deposits come in above the level of the sand plain.

Beekmantown.

Series I to III, The only Pre-Cambrian outcrop in Beekmantown is
found on Rand’s hill, a wide northeast and southwest ridge running from
western Beekmantown into southern Altona. On the east and south, a heavy
mantle of drift covers the flanks of the hill, concealing the extent of the rocks
in those directions. The ridge is made up, for the most part, of anorthosite
which is flanked on both sides by gneiss. On the east is a microperthitic
eneiss of brown color, which contains both green monoclinic pyroxene and
hornblende. On the west the only gneisses shown are basic, very schistose
hornblende gneisses, both with and without pyroxene.

The main interest attaching to the anorthosite here is due, in the first
place, to its distance from the main body of that rock; and, in the second
place, from the information it gives regarding the character of the surface on
which the Potsdam was deposited. At the present time the hill is entirely
surrounded by Potsdam, with the possible exception of a strip half a mile
wide: The summit has an elevation of 1,500 feet, while the Potsdam on the
west side runs up to 1,400 feet, and we are certainly justified in assuming
that at one time the whole hill must have been covered by the sandstone,
quite probably to a considerable depth.

The exposures of the anorthosite in Beekmantown are by no means
as good as in Altona, and the rock will be described in the report on that
township. Those in Beekmantown are of quite typical anorthosite, but the
rock is not fresh.

Series IV. Potsdam sandstone. The only outcrops of this rock seen
in the township are along the road over Rand hill, and closely adjoin the
anorthosite on the west. The exposures are tolerably frequent, but very
poor and the only rock seen is of the red, feldspathic, easily disintegrating
variety. Except for a gap one-half mile wide, occupied by hornblende
gneisses, the Potsdam exposures are practically continuous along the west
side of the anorthosites, and the road is reddened throughout the larger
part Of its length, by the degraded rock. No conglomerates were seen,

East of Rand hill, the very heavy drift-covering completely hides all

rock from view till the Calciferous exposures in the central part of the town

560 Report or tHe Srare Geroxoaist.

are reached. To the south, too, everything is concealed. Much of this
covered territory must be occupied by the Potsdam.

Calciferous sandrock, This formation is better shown as a whole in
Beekmantown than anywhere else in the county. In the central portion of
the town, within a radius of two miles from Beekmantown Corners, are many
exposures, the aggregate thickness of which must be very great. One mile
north of Beekmantown station, is the fossiliferous locality which has been
described by Professor Whitfield,* where beautiful Ophiletas may be obtained
in abundance. The other exposures are of very sandy grey dolomites, some-

times passing into nearly pure white sandstone. All the Calciferous here
seems to belong to Divisions C and D, of Brainard and Seely.+
Southward from Beekmantown village, a well marked ridge of Calcif.

erous dolomites runs southward, and is continuous with the Calciferous

° ry

ae 2
NS Oo) = dam emer

that lies west of the Beekmantown fault in Plattsburgh. The best exposures
are at the Poor-house. The fault passes into this township, but its course
has not been definitely traced.

uxposures along the Lake. Cumberland Head Series. The black slaty
limestones of this series extend into the township from Plattsburgh, and are
exposed along the shore of Treadwell bay and thence westward for a mile.
The exposures form a series of narrow, sharp ridges, the topography resulting
rather from the slaty cleavage than from the dip of the rocks. The fossils
are the same as on Cumberland head.

On the shore at Long point and to the northward, are similar rocks
They have so far furnished no fossils, and require further study, biet are

classed with the preceding provisionally, on account of the lithologie and

* Bulletin American Museum Natural History, Vol. IIT., /p. 2.
! Bulletin American Museum Natural History, Vol. IL, p. 48.

GroLocy oF Crirmron County. 561

CusHING
topographic similarity. They he well to the eastward of the Treadwell bay
exposures, as though shifted by a fault. If that be not the case, they are at
a higher horizon.

Rocks of Uncertain Age. Closely adjoming these Cumberland head
slates on the west, are hard, grey dolomites, which form occasional knolls
protruding above the general surface. In one of the exposures, limestone
bands occur, which are full of fossil fragments, and similar to the bands
described from the upper Calciferous in Peru, just north of Valcour. These
rocks would be unhesitatingly classed as Calciferous, were it not for their
position. It seems certain that they must belong to that group, and they are
so represented on the map. Yet they are separated from the main exposures
of the Calciferous in central Beekmantown by a wide valley in which no

gives no indication of a fault between

exposures occur, while the topography
them and rocks close at hand on the east, which he at least 1,500, and
probably 2,000 or more feet higher in the section. This may be the line of
the Beekmantown fault. It is at least certain that throughout this territory
the entire Chazy is faulted out.

Along the lake shore, from the extreme end of Point au Roches, south-
ward to the hghthouse, are pretty continuous exposures of blue and black
limestones, at times somewhat slaty, but ordinarily massive. They are very
barten of fossils, holding Leperditia in some layers but little else, so far as
found. The top layer at the Point is charged with marcasite and contains
Leperditia and a Holopea-like gasteropod, abundantly. The section has con-
siderable thickness; just how much, remains to be determined, but one hundred
feet is a very modest estimate. The writer is unable at present to indicate
the precise stratigraphic position of these rocks. Mr. Van Ingen writes that
the Leperditia layer at the Point recalls the basal bed of the Black River lime-
stone on Button Bay island, and is disposed to correlate it with that, and to
regard all the rest as of Chazy age. While this is quite probably the proper
interpretation, the entire lack (or apparent lack) of the fossils which elsewhere
in the county abound in most of the upper Chazy, is an objection to it. The
rock closely resembles some beds found in the upper Chazy, but they
nowhere exhibit anything like the thickness shown here. It is therefore
thought that we may here have beds of Trenton age not met with elsewhere
in the county, occupying a position either just above, or just below the
Cumberland head series, and they are provisionally indicated as such on the
map. If they are of Chazy age there must be a considerable fault between

them and the Trenton slaty limestones north of Long point.
36

pt
_~
or
bo

REPORT OF THE STATE GEOLOGIS?.
‘
Such indecisive results are presented very apologetically. The scarcity
of fossils and the lack of time for work of the detailed character necessary are
accountable therefor.

Series V. The eight dikes found in Beekmantown, are all on Rand
hill, cutting the Pre-Cambrian rocks. The proportion of bostonites is greater
than usual, six of the dikes bemg of that type. These show well the very
considerable variation which such rocks present. Dikes Nos. 28 and 29
are of dense, hard red rock of aphanitic, stony look, almost entirely devoid of
phenocrysts, and with very small content of ferro-magnesian silicates. Nos.
27 and 107 have a peculiar schistose appearance in the hand specimen, as if
they had been subjected to shear, but the appearance is entirely lost m the
thin section, which appears quite normal. ‘They contain a larger proportion
of dark silicates than the first two. No. 27 has also abundant orthoclase
phenocrysts of unusual purplish color, which is due to the filling of the
cleavage cracks by hematite.

Nos. 81 and 103-are nearly black rocks, likely to be taken for diabases
in the field unless carefully inspected, but in the slide are quite like the
others except for the presence of a much greater amount of hornblende and
biotite. These occur mainly as inclusions in the orthoclase, and the trachytic
structure is not well defined.

Series VIL Rand hill is so heavily banked with glacial deposits on the
east, south and west, that all rock is obscured by them for a distance of at
least two miles in these directions, and commonly for more. The surface is
everywhere strewn with loose irregular blocks of Potsdam sandstone. These
accumulations may be morainic in origin, as suggested by Mr. Baldwin,* but

no opportunity was afforded for closely investigating them.

Altona.

Series I, Gneiss of the ordinary microperthitic variety 1s exposed on
the eastern side of Rand hill. Its contact with the anorthosite is shown
along the turnpike (old military road) and exhibits a transition zone, a few
feet in width, of a rock of intermediate mineralogic constitution. This
transition rock has cataclastic structure and shows a dike-like dark band
which proves to be a sheared strip, consisting of a finely granular aggregate
of quartz, microperthitic orthoclase, augite, garnet, and a little plagioclase.
The garnet is certainly secondary, and much of the rock has undergone
recrystallization.

* American Geologist, Vol. XIII., p. 181.

CusHING

GEOLOGY oF CuINTON CouNTY. 568

The north end of the Dannemora mountain gneissic ridge projects into
the southwestern part of the township, the rock being the pyroxenic gneiss
usual on that ridge.

Serves IIT. Anorthosite forms the main part of Rand hill here, as in
Beekmantown. Excellent exposures may be seen along the turnpike and
thence southward up the hill. The surface rock is fresher than in Beekman-
town, probably due to the more energetic action of the ice-sheet on the
northern slopes of the hill.

As here shown, the rock is less completely granulated than the Keeseville

rock, in much of which no large fragments remain. Here none of it has

ee
-

ee
Pn FOES
iow aie

js

‘.

eS SS
—

northositfe . Potsdam. Pleistocene .

undergone complete granulation and much of it is quite coarse, so that
the large labradorites, instead of the granular portions, give the main color to
the rock.

Garnet is very abundant, much more so than in the Keeseville rock,
so that frequently the granular matrix which surrounds the labradorite
individuals has a very pronounced dark red tinge. Some portions of the
rock consist entirely of garnet and labradorite. Generally, however, augite

and magnetite are also present and hornblende is common. Hypersthene has

564 Report oF THE STATE GEOLOGIST.

not been observed here, nor in any of the anorthosite in the county. As was
to be expected from the less complete granulation, but little of the rock is
fohated, the basic minerals occurring in clumps rather than in streaks.

A short distance up the hill from the turnpike, a well foliated gabbro
outcrops. Owing to the tangle of brush and the thin soil covering, its extent
could not be determined, but it is not great. It is less basic than the ophitic
gabbros, and lacks that structure; neither have the uncrushed labradorites
the abundant inclusions which characterize those of the ophitic gabbro,
Besides the labradorite the rock contains much garnet and magnetite, consid-
erable apatite, and what was probably augite now wholly passed into chlorite.
Granulation is not complete. The labradorite crystals which have partially
escaped this process, show beautiful polysynthetic twinning, and exlibit most
notably effects of the dynamic action other than the granulation. Not
only are they broken and the fragments displaced, but nearly all are bent,
the bending being most clearly brought out by means of the oft-repeated

twinning, as shown-in the accompanying figure drawn with the camera lucida.

Broken and bent labradorite crystal from gabbro on Rand hill, Altona. The surrounding granular
material ig almost wholly labradorite.

Series TV. With the exception of the small areas just noted, the Pots-
dam sandstone is the surface rock throughout the township. Moreover, here
is by far the most impressive display of this rock to be seen in the county,
if not in the state. Extending north from Rand lil] is a plateau of nearly
horizontal Potsdam sandstone, running up to heights of 1,100, 1,200, and
even 1,500 feet, and stretching away northward with an average fall in level
of from seventy-five to one hundred feet per mile. For the most part it is
very bare of debris, and on the steeper slopes the naked ledges of stone rise
in a series of gigantic steps, as if they had been swept bare of debris
by powerful currents. The district goes under the name of the “Flat
rocks.” It is rather deeply incised by the Great Chazy river but otherwise
is not deeply dissected by erosion, appearing as a base level of tolerably

recent elevation. Rand hill is a monadnock rising above this level.

CusHING—GEOLOGY oF CLINTON CouNTY. 565

It is very difficult to get any trustworthy conception of. the thickness of
the Potsdam as here exposed. The rock lies in a series of slight north and
south folds, with such a shght dip, that it is no easy matter to determine the
amount of pitch. The pitch is quite certainly to the north, and somewhat
in excess of the fall of the surface in the same direction. The floor on which
the rock was laid down also falls to the north, and at a greater rate than the
dip of the rock.

Heavy basal conglomerates, such as those in Ellenburgh, make but little
show in Altona, very possibly because of the lack of exposures in the vicinity
of the crystallines, though this can not be the whole reason. Several outcrops
of small extent, but occurring within a few yards of anorthosite or gneiss, are
found on Rand hill, and are all of red, feldspathic, easily degraded type, with
no sign of conglomerates. Away from the crystallines the rock presents its
usual variations in color, size of grain, and degree of induration.

Series V. The most impressive display of dikes to be seen in the county
is exhibited along the turnpike where it passes over the northeastern edge of
Rand hill. The anorthosite here is seamed with dikes, some of which are
very large and complex, branching repeatedly and covering considerable
territory. These vary so much from place to place that measurements five
yards apart would give wholly different results, but the complexity is well
illustrated by the following careful measurement of a portion of Dike No. 8,
made along the surface in a north and south direction. Commencing at the
south is

1. Anorthosite,

ee inser weer, eat ene eS ft. 1 im,

DEP NOLUNOSIEe Geter ewes - <<. 11. * 9 “

en De Ase we ener ere ete Li tae sy Ore Qe

De AMOVUNOSILC meet nase eaten weg a LG O°
| enclosing three small

pee iaaccoaneee ieee eee... 25-8." 4. horses of anortho-
| site.

[EP ANOrNOse ee ereGrec et. .. - « 91 “4

See a Desc nEnmere uate hen ete The LE 10-

OS) ut LNGLETLIVOISD USS 0 oe ot ney

IDS” Lose TASES eT eA ie an pcre a

He MOrenOStteme ct iag en tata. GL OOM

Ree icew remem a ror oie ee, A SOO

13. Anorthosite,

566 Report oF THE STATE GEOLOGIST.

The sub-divisions of this dike bear in all directions, re-uniting and
forking again, so that several of the anorthosite members of the section
represent enormous horses in the diabase.

Fourteen dikes have been found here within an area of less than a square
mile, and if all the branches were counted separately this number would be
trebled. The heavy second-growth on Rand hill undoubtedly conceals many
more. The only two of these dikes that call for any especial mention are the
two bostonites.* No. 7 is of the red, aphanitic type, with numerous small
porphyritic orthoclases showing. It contains a little magnetite and chlorite,
and the flow structure of the ground-mass is well marked. No. 9 represents
the other extreme of these rocks. It is coarser, the whole appearing holo-
crystalline to the eye. It is much darker in shade, due to a large biotite con-
tent. Both orthoclase and biotite occur in two generations, the orthoclase
phenocrysts reaching a length of over one centimeter. The ground-mass is
quite coarse, and contains apatite and augite in addition to the orthoclase
and biotite. Quartz has not been recognized ; if present it is only sparingly
so. This is the only dike of this type so far noted in the region which has
phenocrysts of a ferro-magnesian mineral, and the great abundance of the

biotite in this dike is quite unusual.

Chazy.

No Pre-Cambrian rocks appear in Chazy township.

Series IV. Potsdam sandstone. ‘The Potsdam occupies the north-
western half of the township. That on the extreme west belongs to the high
plain and pertains to the basal part of the formation. That on the low
grounds, on the contrary, is toward the summit, the passage beds to the Cal-
ciferous appearing just over the border in Champlain township. <A great
fault separates the high level from the lower Potsdam, and another great
fault les between the Potsdam and the Ordovician limestones to the east of
it. Most of the rock is of the ordinary character, and calls for no comment.
A curious black layer, several feet thick, is exposed in a railroad cut Just north
of Chazy depot. While mainly a quartz rock, occasional grains of orthoclase,
microcline, plagioclase, hornblende and magnetite occur, and large zircon
grains are a feature. The quartz is full of minute black inclusions, and
there is also a black cement of uncertain nature to which the color of the

rock is due.

* Trachytes would be a better term as that is what the rock is, and no useful purpose is served by the use of the other so far
as the writer can see, It is used here merely to make the nomenclature conform to that already in use in the region.

GEOLOGY OF CLINTON CouNTy. 567

CUSHING

Calciferous sandrock, This formation, which is so widespread in Beek-
mantown, just to the south, makes but little display in Chazy, appearing only
in the extreme south, where the upper beds are shown, soon to be followed
toward the north by the Chazy. The exposures are poor and possess little
interest.

Chazy limestone. Here is the type locality of the Chazy, and nearly the

.

whole of the formation is exceedingly well shown. In the near vicinity of

. oa0o0 6
} 3 [ee 06

By,

EF ----[-| [eecclsecece|
FE=--F=- =] e]eeceelaed ae

Potsdam alci}erous. Chazy. Trenton. Leistocene.

Chazy village it has been carefully sectioned and mapped by Brainard and

Seely. For convenience of reference their section 1s here repr dduced.*

MEASUREMENTS AT CHAZY IN ASCENDING ORDER.
Group A.
1. Iron-grey, fine grained dolomitic limestone, in beds one or two
feet in thickness, weathering drab with fine yellowish streaks at
right angles to plane of bedding containing Orthis costalis and

D?)

Gumiaidalgenaopacnusaiins aad ribet Ces ne ie eee o ALO TE

* American Geologist, November, 1888, p. 324.

568 Reporr or THE Sratre GEOLOGIST.

6.

Tolerably fine limestone, filled with fragments of crinoids, con-

taining Orthis-and Strophomentm, “.))2 20a eee ee 20 ft.
Measures concealed; i.) Ss. Sid 41 A ee ie a ee te

Impure limestone, filled at bottom with Orth7s, thin-bedded when

long exposed to weather, the upper six feet abounding in

ermoidal fragments; . <5. 020 57 So aah ies ip Ol eel sere
Fine-grained, massive limestone containing Scalites angulatus,

Kaphistoma and fragments:of tnlobitess 2 2 ee
Impure limestone abounding in Ovihisi= =2—. ii
Measures concealed; 50". -.> "4. 22 eel ee ee

Massive grey limestone, largely made up of crinoidal remains,
having red spots in a stratum about ten feet from the top;

abounding with gasteropods near the middle, ... . . = . . 50 @

a KOE ns
Group B.
Thick-bedded, nodular, dark-colored limestone, — containing
Machurea- magna, oS Ee, Gee eee
Massive, pure limestone, grey, fine-grained, often odlitic, abounding
in crinoidal remains and Stenopora fibrosa,. . . . . . . . 20%
Massive, bluish-black, tolerably pure, nodular limestone,
containing Waclurea magna and masses of black chert, . . . 45 “
Similar to No. 3, but containing in addition to Maclurea, various
species of Orthoceras and large masses of Stromatocerium, . . 90
Less massive limestones, quite impure, and often disintegrating

into nodules as though shaly, 7: --0.5 2 = eee oa em

Group C.
Dark, iron-grey dolomite, weathering yellowish,. . . . . . . Ub a
Blue, compact, fine-grained, pure limestone, containing fine lines
of calerte, 2.0 455 Se eee

Dove-colored, compact, brittle, perfectly pure limestone, contain-

ing small nodules: of :calette,s:- ete ae ace eee eien cn ene Bae
Iron-crey dolomite, '*i/:) <iCgah eee — fap) ees eee oat
Like No. 3, only containing larger calcite nodules,. . . . . . 43‘

Dark-grey, fine grained, compact limestone, somewhat impure,
having a mottled aspect when weathered, containing undeter-

mined species of Murchisonia and Orthoceras, . . . . . . 2

Cusntne—GroLocy or Crinton County. 569
fs Tron-grey COG remiinc Mara mere nee totes! ce hi eat? DY ea ey Lett:
8. Blackish, impure limestone, abounding in Rhynchonella plena, . 8644
9. Grey, massive, coarsely granular limestone, mostly made up of

crinoidal fragments, which are sometimes red, containing
ie) ae Men REBATE ds oleae con DOR
om eait race Nowe we ee ieee! ei ae Ter ieee ek a oe at BO
ie WicaoumecscOncealed, Seren wiee dhe eo. ks ass
PA non map Uuredolomitew ss Mees ie toe me ee a Sint
pe eer UmeNicONCemleGnssiain mctuete si ee a SS ee te OAS
Loy Lit
Mota muMnckinessOre Nw and Cre... oy wl wy) BDF.

In the southern part of the township the lower division of the Chazy is
widely exposed, especially toward the west, but it is much disturbed there,
and no section has been seen as good as that quoted. Running due south
from Chazy village, and lying just to the east of the territory included in
their map, is a long section of shght dip, extending unbroken from the Calcif.
erous up into the basal Trenton, though much of the upper and lower
divisions of the Chazy are not well exposed. It is the only section in the
county, except the one on Valcour Island, which shows the entire Chazy,
but it is not well adapted for a determination of the thickness on account of
the shght dip.

Some layers of the Chazy were formerly quarried in the township for
building stone, but the industry has lapsed, probably because of the better
quality of stone obtainable from Isle la Motte.

Black River limestone. Nowhere else in the county has this rock been
found well exposed, but it is admirably shown around Chazy village, and is
quarried and burned for lime on a large scale. It is a compact, ringing,
massive black limestone, much of it with conchoidal fracture, and has a thick-
ness of thirty feet. It is quite fossiliferous in some layers. A bed twenty
feet from the base contains a large Maclurea and masses of Stromatocerium,
much like the Chazy forms, so that when this layer alone is exposed, it is no
easy matter to distinguish the two. Coluwmnaria is confined to one or two
layers just beneath the Maclurea bed. Beneath the beds are rather barren,
but hold Asaphus gigas and lJamellibranchs identical with Trenton forms,
At the base is a Leperditia layer, and the whole rests on a massive, brittle,

dove-colored limestone, with conchoidal fracture, which forms the summit of

570 Report or THE STatTE GEOLOGIST.

the Chazy, and is missing from Brainard and Seely’s section, The rock is
very like No. 3 of Division C, of that section.

Trenton limestone. North and east from Chazy village, the lower portion
of the Trenton is found exposed, a thickness of about 150 feet being shown.
The best section is that in the Little Chazy river, Just east of the village,
where the dip is high, so that within a short interval, a considerable thickness
of the rock is exposed. Alternating beds of black, rather slaty limestone,
and more crystalline beds of lighter color, which are full of brachiopods,
make up the section. They are in all respects similar to the lower beds on
Crab island and in Plattsburgh, but here in Chazy is the only locality found
in the county where the Black river and Chazy limestones may be seen in
place below them.

Faults. Owing to the better and more frequent exposures, the faults
which have dislocated the Palaeozoic rocks are more readily worked out in
detail in Chazy than elsewhere in the county. They have already been
discussed by the writer, in so far as the stage of the work would permit.*
The past season’s work in company with Messrs. Van Ingen and White
corrected : inaccuracies in two Instances, and later on some other errors were
found.

The most conspicuous and important break shown in the vicinity, is the
great fault running across the township from southwest to northeast, and on
into Champlain township. It will be called the Tracy brook fault, as the
entire course of that stream lies along the fault line. Along its course
through Chazy the entire Calciferous is blotted out, the various members of
the Chazy and even of the Black river being brought down against the
Potsdam. The entire throw is not far from 2,000 feet.

The downthrow block on the east of this fault is much shattered, and
consists of a series of small blocks caused by cross faults. The dip is steep,
ten degrees or more, and the amount of throw is ordinarily to be determined
with ease by the surface shift of the Black river limestone, which forms the
most convenient horizon for this purpose. Seven of these cross faults have
been identified in a distance of three miles, and doubtless others will be dis-
closed, as detailed mapping is extended southward. This shattered zone is
terminated eastward by another fault, which closely follows the course of the
Little Chazy river, and may therefore be called the Little Chazy fault. But
to the north and south it passes into drift-covered territory, beyond which

it can not be traced. East of this fault is the long continuous section

* Bulletin Geological Society of America, Vol. VL., pp. 285-296.

on

Cusuine—GroLoay or CLinton County. 71

of the entire Chazy, followed by the Black river and ‘Trenton, which
has already been noted. The structure is that of a low anticlinal with
northerly pitch.

Still farther east, the Chazy beds are cut off abruptly by an apparent
fault at right angles to the strike. No rock shows to the eastward but there
is an abrupt fall in altitude of from sixty to eighty feet. This probably
represents the northward prolongation of the Beekmantown fault, but has not
yet been demonstrated as its equivalent.

Series V. No dikes have been found in the township.

Series VI. Besides the long esker already mentioned, nothing worthy
of special description has been noted. The Champlain clays are found

everywhere except on the extreme west.

Champlain.

No pre-Cambrian rocks occur in Champlain.

Series IV. Potsdam sandstone. The Potsdam extends into Champlain
from Chazy along the west side of the Tracy brook fault. It 1s exposed
quite continuously along the fault line as far as Cooperville. From that
point northward, dolomites appear interstratified with the sandstone, marking
the passage beds to the Calciferous, and followed by the heavy grey dolo-
mites of the Calciferous itself about a mile north of Cooperville. These
continue to the Canada line, the whole with slight northerly dip.

This strip of Potsdam and Calciferous along the west side of the Tracy
brook fault, has a width of from two to three miles, and is adjoined on the
west by territory in which nothing but Potsdam is found clear to the Canada
line, the dip being slightly to the north, as before. Not even the passage
beds are seen on the west. ‘There is clearly a fault here running the ful
length of the township in a nearly north and south direction, and throwing to
the east. The amount of throw is purely conjectural as the horizon in the
Potsdam on the west side is not known, but it has an undoubted mimimum
ralue of 250 to 300 feet. The name “Champlain fault,” is suggested for it.
Continued to the south into Chazy with the same trend, it would connect
with the Tracy brook fault near Chazy village, the junction of the two
furnishing an adequate explanation for the prominent ridge of Potsdam with
abnormal dips which lies west of the Tracy brook fault north of Chazy
village.

Caleiferous sandrock. ‘The Calciferous exposures in Champlain are

limited to the zone between the Champlain and Tracy brook faults. As these

572 REPORT OF THE Strate GEOLOGIST.

diverge somewhat, the width of outcrop widens northward. In this zone
meagre exposures are not infrequent, but do not suffice for the construction
of a section. It seems, however, that only the lower division of the formation
is represented. The rock is mainly a hard, massive, grey or iron-grey dolo-
mite, but is often very sandy, and in some layers the sand predominates, and
the color is lighter. The sand is mainly coarse, and often gives a pseudo-

oolitic appearance to the rock. One mile and a half west of Rouse’s Point, a

Ay |
al

Es

leofeoe ee ele)
Calciferous. Chazy. Trenton

layer of coarse breccia is exposed, the ordinary grey dolomite containing
numerous, rather angular pieces of finer grained, more sandy dolomite, of
varying size up to four or five inches in length. These pebbles, if they may
he so called, are clearly derived from the formation itself, being precisely like
layers which oecur just beneath the breccia at that point.

Chazy limestone. A portion of the Chazy is well exposed in the district
from Cooperville eastward to King’s bay. Nearly the entire Maclurea divi-

sion and much of the lower division are well shown and very fossiliferous.

GEOLOGY OF CLINTON CouNTY. 5

CusHING

The average dip is ten degrees to the east, while the Potsdam, less than a
mile to the westward, has a slight northerly dip, the Tracy brook fault lying
between. What is known as the King’s bay quarry, is here in the Maclurea
beds, and formerly considerable stone was taken out here.

Three miles further north, and about two miles southwest of Rouse’s
Point, another ridge of Chazy limestone protrudes above the surface, and has
been quarried somewhat. Only a few feet in thickness of the Maclurea
beds are seen here. They have the same easterly dip as at King’s bay,
though steeper, while on the west are nearly horizontal beds of the lower
Caleiferous, marking the further extension of the Tracy brook fault.

Trenton limestone. The road south from Rouse’s Point runs for two
miles just east of a low rock ridge, covered only skin deep by soil. A small
opening in the rock, about two miles south of the Point, discloses Black
river limestone, striking with the ridge, and therefore probably forming the
whole of it. The dip is in the same direction as is that of the Chazy, a mile
to the westward, so that both probably hein the same fault block. This is
the only exposure of undoubted Trenton (inclusive of Black river) in the
township known to the writer. Just to the east, and occupying the larger
part of the peninsula north of King’s bay, is a considerable marsh which marks
a fault line, beyond which are exposures along the lake shore at Stony Point
and Point au Fer. On Stony Point is the Utica slate, as already described.
At Point au Fer is a rocky cliff, extending several rods along shore, and
exposing from fifty to one hundred feet of rock, the lower portion consisting
of dark blue, somewhat slaty limestone, much jointed and with the cracks
commonly filled with calcite; while the upper part is well laminated and
quite argillaceous, splitting into thin, even slabs, and weathering to a light
color. No fossils were found here, and the stratigraphic position of the beds
is doubtful in so far that it is uncertain whether they belong below or above
the Utica horizon. They are certainly not older than the Trenton, and are

provisionally mapped as of that age.

GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

PRELIMINARY REPORT ON THE GEOLOGY OF ESSEX COUNTY.

JAMES HALL, | Jah KEMP.

State Geologist. Assistant.

1895,

575

James Haut, State Geologist,

Sir:—I submit herewith a continuation of my previous report upon
the geology of Essex county, and with it geologic township maps which
almost complete the survey of this county. Small areas still remain in the
extreme northwest and on the southwest which, on account of their wild
nature and inaccessibility, | have not yet been able to reach with the time
and means at command.

Very respectfully yours,
Jo KEMP:

&

re a ' ATA,

= — ra pope cing eS
4 Pigs ek iz

+4 % % ) joes? ut
aloe te ¢ ,

oe
& te 7
to en*
i
" moe
ms
Be. 4
-
ae

J i f
a j ‘“ yl f wetkin *
¥ ey ti W ¥ ee He eH re at z

; 3 J em” fy . AV

a
ied
i
4
”
i> 5 > ,
<a hry * hy Mme
Ta NS, Se SS
ane ope
3

‘
)
4
}

i]
s
ee ee ee
PF

$]
\

:
{

me is
p
4
=
*
Fito, q
andes
hen aad R

te
P oat

a. A
A
arn
i“
:
‘
a
5 rig ts
bis
| 4

;
A
y
2+

x
;
so)
3 «
zee P, :
’ ; :
“ J
ye ee ee >
ogee: aT A
. \ § v
~ ae. . f
i Se ff
YY
-
i,
“
i
— eee ee ee

ff
wR ae,

Map oF ESSEX COUNTY,

Preliminary Report on the Geology of Essex County.

By J. F. Keme.

(Continued from the Report of the State Geologist for the Year 1893, pp. 433-472.)

The field work for the accompanying report was done in September,
1894, and September, 1895. In the former month a trip was made from Port
Henry across North Hudson and Newcomb townships and into the old iron
mining settlement at lake Sandford at the expense of the Geological Depart-
ment of Columbia University. In September, 1895, the field expenses were
borne by the State. Almost indispensable aid has been afforded by the
topographic maps of the United States Geological Survey, so far as prepared
or available, but the western townships have not yet been mapped in this
way, or at least have been drawn only along their eastern borders, and the
lack of an accurate location of water courses and boundaries has been felt in
these districts. Acknowledgments are due to Mr. Herbert M. Wilson, of that
Survey, for his courteous and prompt supply of advance sheets.

The same series of signs and the same provisional nomenclature that was
used in my former report has been continued in this one, and to those intro-
ductory pages, 444-451, reference may be made for their full elucidation.
For the sake of clearness, however, a brief outline of the several divisions
is here repeated. The additional observations have corroborated these previ-
ously published generalities, but it is doubtful if a sharp stratigraphic
distinction can be drawn between Series I and II. It seems increasingly
probable that the crystalline limestones may prove to be but phases, perhaps
several times repeated of Series I, but they are lithologically distinct and
pecuhar. They are noticeably more abundant to the south and southwest.
In this connection results to be obtained in mapping Warren county are to
be awaited with interest.

Sertes J, Gneisses usually with both orthoclase and quartz. Varieties
with hornblende, biotite, pyroxene, and with almost no dark silicate. are met.
Plagioclase is usually present and may be the only feldspar. The exposures
vary in color from very light grey, almost white, to dark grey or even to red.

The lamination may be conspicuous or may almost fail.
579

580 Report oF THE SraTE GEOLOGIST.

Series II, Crystalline limestones, ophicalcites, black hornblendie-
pyroxenic schists and thinly laminated garnetiferous gneisses.

Series III, Rocks of the gabbro family, ranging from aggregates of
pure labradorite through varieties with increasing amounts of dark silicates
to basic olivine-gabbro. The varieties rich in feldspar are called anorthosites,
following the Canadian practice. They shade from perfectly massive varie-
ties into others strongly gneissoid.

Series IV. Palaeozoic sediments, viz., sandstone, limestone and _ shale,
of which the Potsdam of the Cambrian is the oldest and the Utica shale of
the lower Silurian is the latest.

Series V. Trap dikes and porphyries.

Series VI. The glacial and post-glacial gravels, sands and clays.

In the subsequent descriptions a topographic sketch is first given of the
town, and then the several series are taken up in the above order. The iron
ores or other economic products conclude the local notes. The townships are
described in general from north to south, as follows:

Chesterfield (revised), page 580 Schroon, 9° 3-2. pave aoe
Jays. Oke eer Osi Ticonderoga (revised), “ 600
Wilmington, . . . 1G SD Minérva, "ose “600
Sty Aumrands eer Paes Newcomb; os =: “604
) ?
North Hudson, . . 2H OO
Chesterfield.

In my previous report, a map and description of Chesterfield were given
on page 463. The map was based on the county atlas, as the Willsboro sheet
of the United States Geological Survey had not at that time appeared. I was
misled into thinking that the western line of the town lay just beyond the
valley in which is Trout pond, but the new maps, especially the Ausable
sheet of the United States Geological Survey, and field work along the border
from Jay, have shown that another valley and brook lie in the interval and
that the gneisses extend across this western boundary, as far to the east as
Clintonville, embracing on the south the little crystalline limestone area, and
projecting into Jay.

The rocks on the south are puzzling gneissoid types, but after a trip
across the southwestern corner of Chesterfield to Bluff mountain, in Lewis
township, and observations on the trend of the ranges, I am led to redraw
Chestertield as in the accompanying newer copy herewith submitted This

also has the drainage correctly drawn and in much greater detail.

PLATE I

SY A
ES TOR ARs
PRUE Sy BRBREE
AAO ENA RARE'
LORRY. eae

VV \
ARABARARR
KAAS

x LAA

QuaBeaaae'
AR EBBE

<M aay.cuwue
: SALA
Que

TA

VAM SS

NAAR, WBABAt ARABS
ASS Ne

VW
AB ARRRBABASa'
ABRSARBRRT RET “A
ea Ay VS

%2 GNEISS CRYSTALLINE ANORTHOSITE GABBRO CAM
STA BRIAN LOWER SILURIAN GLACI
LANNY RASS BSSSS5) a I Cae ae atone
ol r POTSDAM SAND urea” GRAVELS ETC,
Se SCALE OF MILES

ANORTHOSITE OR GABBRO
GEOLOGIC MAP OF CHESTERFIELD TOWNSHIP.

=) ; i a
i
i
- ;
'
r
i
’
1 c
j
‘
‘
'
“
‘
5 i
‘
2 U y y
\ >
sy
i 5
= om
“|
F i ne
F : ;
: yo 3
. t
t
i
‘ a =
/
& "d
“s at
re) u :
i)
it =)
Det =
1 ~ ‘¢
t
1
a ,
=} i
‘
t t
t
t
, 4!
"
I
$
\
2
‘
be
i
, ‘
as
’
a 1
4
1

Kemp—GroLoGy or Essex Counry. ‘ 581

SS)

The western border of Chesterfield is a very wild, rough and mountainous
district, and needs more detailed study to make the delineations of the for-
mations of other than a general character.

Series I, On entering Chesterfield from Jay, the area of rich quartzose,
feldspathic gneiss that is extensively developed in the northwestern part of
the latter town, runs across the border. I went up over Bald mountain, and
collected specimens 11 and 12. In thin section they exhibit quartz and
microperthitic feldspar, with the dark silicates in No. 12 only represented by
decomposition products. The quartz is especially rich and is rolled out in
lenticular masses.

On the north side of Bald mountain, is the wild gulch called the “Gulf,”
and south, still further, and on the east side of Black mountain, is another
ravine scarcely inferior. Plumbago prospects are reported in the “Gulf,”
from which I saw samples that would suggest the probable presence of
crystalline limestones as well; but from pressure of time and the necessity of
traversing the southern side of the county to get the broader geologic
features of that section recorded, I was unable to fully explore the region.

The gneiss extends south from Chesterfield into Lewis township, and at .
No. 42 (of the Jay map) appears in the high, rough ridge of Bluff mountain,
and at No. 43 in the outlying spur of Jay mountain on the south. Both of
these specimens, in thin section, show much quartz, with which, in No. 42, is
strongly microperthitic untwinned feldspar, and a few shreds of nearly
opaque hornblende. In No. 48, quartz is in excess. With it occurs much
augite, some scapolite, and almost no plagioclase. Regarding the other series

of rocks, no new facts have been noted.

Jay.

Jay is a very irregularly shaped township, as the map indicates. Its
greatest length is about thirteen miles from north to south, and except in the
narrow extension into the wild mountainous country in the southeast, it
averages about six miles from east to west. The greater part of it lies in a
valley along the east branch of the Ausable river. The valley is open and
broad on the north, where the surrounding hills are two to three miles apart,
but on the south they close in decidedly and, at the line with Keene, the valley
is narrow. The altitude of the river varies from 550 feet A. T., at Ausable
Forks to about 700 at the Keene line. Except along the main stream of the

Ausable river on the northeast, the border line with Chesterfield is a very

582 Report oF THE STATE GEOLOGIST.

wild and mountainous strip; Bald mountain is 2,139 feet A. T., but less than
a mile south of its summit the Gulf runs east and west like a gash, and at less
than 1,000 feet above sea level. The northerly spur of Black mountain, at a
short distance from the south side of the Gulf, is 2,100 feet. Without careful
study I regard this as one of the faulted valleys to which reference was made
in-my former report, p. 439. The main summit of Black mountain is 2,160 feet.
It is separated by another wild gorge from an unnamed peak southwest of it
that attains at its summit 2,632 feet of altitude. Still further south is Jay
mountain, 3,287 feet in the town itself, and 3,601 feet just across the line in
Lewis township. At the extreme south the northerly spurs of Hurricane
mountain reach an altitude of over 3,500 feet. About three miles southeast
of Ausable Forks, a knob-like hill called Haystack rises to an altitude of
1,338 feet. From the west its outline well justifies its name. The western
town line runs along near the summits of several rather large hills of
anorthosite which are separated by cross valleys. The northerly one, Clark
mountain, is 1,577 feet, the next one south called Hamlin mountain, is 2,122
feet, then follows Bassett at about 1,900 feet, and Ebenezer at about 2,000 feet.
Southwest of the town is the huge mass of the Sentinel range, and just inside
the southern line of the main portion of the town is Clements mountain, 2,540
feet. On the western side of the southern extension, the contours on the
slopes of Big Crow mountain range from 2,000 to 3,300 feet. It is evident
from this outline that the easily accessible portions of the valley quickiy rise
to the decidedly elevated and wild ranges of mountains, on the east and west,
which are from 1,500 to 3,000 feet above it. In scenic attractions the valley
is one of the loveliest in the mountains.

Series I, The gneisses constitute the northeastern corner for three
miles or more south of the Ausable river. Their strike as shown on the map
is variable, being north and south, northwest, northeast and even east and
west when corrected for magnetic variation. On the east, the rock is a very
coarsely laminated variety with very abundant lenticular masses of quartz up
to two or three inches long, that lie between corresponding lenses of red
feldspar.

In thin section the feldspar proves to be microperthitic orthoclase,
or microcline in largest part. Dark silicates are subordinate, with hornblende
the commonest one present, but biotite is also often seen. Nos. 5, 6, 9, 10, 11,
12 and 13 are of this character. Just across the bridge over the East Branch
at Ausable Forks, a dark green gneiss outcrops in the bank at Nos. 1 and 2.

It looks much like the rocks of Series III, but in thin section it is seen to

TRAIL Lae

GLACIAL

GRAVELS ETC.

z st
<oaice
. = fy cf 2}
ee ail
ELBE SEE. ctf
Z Be A 5 tet
SESE ZEA ‘i 4
LONI Ze | oe
KV YQ SE = | 2% \. e Benita
CIRO LGA tr) aS
RON ERXN ir is { ff JK Ste
BORA ORR OR ZA BOX, A a = |i |
OAR eR RN OR OR =a A a os
ROHN RMN SRN Bg)
ANY ORK PAIK KORN eR RAINY 9 SR, pec Qoa wil 2
PRION CRE lo MN on SLE
F KR MOR ROEDERER ROCK RX CRORE & bX 3
z RORY OK RR PRR PER RRA Kh KOON BR S| 5
A DOR ORDO IES HAM PRONRIURN SE |
2 fe Oi DHA : AN AON, BS oe
ROO LO YY TRIN BLE XK) i 01 3
LT TR RE SRS Mine |g
RAK ARID AB RSE a a MEER ARC PH ABRC ORR NONOXXNYR GIR 3
=o (as Mun Ds UH SN Le ah CoD eR a :
oN KOI BARA KY OLX RO CLI COKER ROOK rae AMY = be S
A ee RR RONAN SUE INO CPX OKRA KIN KOK HOO. EB :
Ne Ns ROOM TREN SRR ROR ORIN ARK OP RAR I RERARR RIOR AA XIORR OY.
re: RRP RIK OA N AM RIN XL 5 eee ea lias wy A Wd, XY ‘ % G NOR” 5 RY
oo Sn AY MOXOS Oy Meme, Nor BRAK HAKRRN ROY RY KLIN Z
RXR R NM XR RRA ROR KALORIK)
RRR RRO RR LILI HX OR OR RAL ALR 2
MONI AMMAN Mie PERL. RRR b
Fo NNN et AUNT Gd pe SANNUSUALIN ONCAOOUU CRM Bpy Fe
FORMA KX XN Be Nae se WE roe Me) 202s
NUNN Una GY ery MY AOAARAAX AL aca
MK? WU XLEX OZ XK en OOK oxy) 7,0) Oe XX Ah a nx
LIEGE MMR GRIN SATS
RBA CERO! \ BEE
cor ye yas” 2
. LLY rag g za es
ak, OX
wh4 aie
zi4 alts
SA 2s .

584 Report or THE SrarE GEOLOGIST.

and a basic garnetiferous, gneissoid rock (No, 40) were in the same ledge and
not over one foot apart. No. 41 is a gneissoid variety again. On my return
from this trip into the mountains my horse ran away and spilled these
specimens all along the highway, so that I lost them and cannot give the
mineralogy more accurately for this reason. At Nos. 55 and 56, gneissoid
anorthosites again appear that show in thin section the familiar crushed
feldspar, and in this case a little hornblende and diallage. Away down in
the southeast, gneissoid norites appear, that contain labradorite, hypersthene,
emerald-green augite, hornblende and garnets. A little quartz also appears,
and a tendency in the plagioclase to develop a microperthitic texture that
resembles the rocks regarded as members of the typical gneisses. Inter-
mediate varieties of this character are extremely difficult to satisfactorily
place in stratigraphic relations, and lead one to concede great possibilities to
metamorphism. The aspect of the rock, however, is clearly igneous and its
relations are with Series III. Another extended stretch of gneissoid rocks is
in the ridge on the east bank of the Branch above Upper Jay, and extending
into Keene. Under the microscope, No. 35 exlibits brown hornblende, a
little green pyroxene, more or less crushed labradorite and deep pink garnets.
It is considered also to belong to Series IIT.

Two exposures of dark basic gabbros have been met in or near the town.
One, No. 4, in the northeast, was not over twenty-five feet thick, in quartzose
gneisses on each side. It is a typical gabbro like the one near the Cheever
mine, at Port Henry. The second exposure is in the town or near its line in
Lewis township, on the southeast. In the thick woods above Sprucemill
creek, appears a large exposure of dark green olivine gabbro, No. 59. The
familiar reaction veins between the feldspar and the ferro-magnesian silicates
are present.

Series IV. The Palaeozoic sediments fail entirely in this town. The
Potsdam sandstone to-day is not found much farther up the Ausable river
than Keeseville, unless it is buried under the sands and gravels, but it 1s not
improbable that it has had a more extended outcrop in earlier time.

Series V. No diabase or other related dikes, except the gabbro described
under Series [II above, were met.

Series VI. The great deposits of sand and gravel that were mentioned
in my previous report, page 464, and that are especially well developed along
the Ausable river, cover a goodly portion of the northern part of Jay.
Especially on the flanks of Clark mountain and in the neighboring parts of

Wilmington they spread out as stretches of sand, covered by a second growth

Kremp—Gronocy or Essex Counry. 585

of timber. Clay is found one mile and a half above Ausable Forks, on the
East Branch, in a thick bed just west of the road. East and south of Hay-
stack mountain, along the highway, are extended deposits of sand that remind
one much more of the seashore than of the mountains. Now that the contour
maps are available, these deserve careful study as illustrating the glacial and
post-glacial history of the region,

Glacial striae are not lacking and are marked in several places on the
map by large arrows. The pilot charts of lake Champlain give the magnetic
meridian as 11° 45’ W. of the true north. The striae have been corrected
for this by making the true strike 12° east of the recorded magnetic. Near
the Forks they run nearly east and west (N. 92° E.). At Lower Jay they
are N. 52° E., and again two miles east, N. 52° EK. Southeast of Upper Jay,
at No. 56, they are N. 12° E. The frequency of boulders of Potsdam sand-
stone well up in the mountains and south of the outcrops of this formation
leads one to infer that there was movement from north to south even against
the present slope. All around the mountains these boulders have often
attracted observation in elevated and interior positions.

Concluding remarks. Much further detailed study is needed along the
Jay-Chesterfield line in the stretch of mountains forming this wild and
uninhabited strip. The writer appreciates that the delimitations of the for-
mations given in the map are based on scattered observations, which future
study may more or less modify, but as a general expression of the results of
a reconnaissance, they are presented because they throw some light on a little

known regi yn.

Wilmington.

Topography. The topography of Wilmington is closely parallel to that
of Jay. A broad valley at the northern boundary with a general altitude of
800 to 1,000 feet above the sea, narrows toward the south or rather southwest
to a mere gulch. Where, as in Jay, we have the East Branch of the Ausable
river, in Wilmington we have the West Branch, a very similar though some-
what smaller stream. In the eastern central portion there is also a marked
side valley along a small tributary which, however, is closely parallel in
direction with the main stream. The mountains that separate Wilmington on
the east from Jay, viz. Clark, Hamlin, Bassett and Ebenezer have already
been referred to under Jay. Between each pair there is a cross valley and

road. The whole southern part of the town is occupied by the rugged and

586 Report oF THE STATE GEOLOGIST.

wild mass of Sentinel mountain, whose extension forms a notable ridge to
the south. The highest point is 8,858 feet, but there are two or three others
that are nearly as high.

The western part of the town is occupied by the noble peak of
Whiteface mountain, whose isolated situation to the north of the other peaks
of the first rank, makes if in many respects the most striking of all the
Adirondacks. The view from its summit yields to that of no other in scope
and grandeur. The summit is 4,872 feet above tide, so that Whiteface is,
according to the maps of the United States Geological Survey the fifth in
altitude of the Adirondacks. Marey, 5,344 feet; McIntyre, 5,112 feet; Sky-
light, 4,920 feet, and Haystack, 4,918 feet, surpass it; Dix, 4,842 feet, Basin,
4,825 feet, and Gothic, 4,738 feet, follow in order; but after Marcy and
McIntyre all the next five have insignificant differences. Whiteface was
thought, for many years in the early part of this century, to be the highest of
all. To the southwest it drops off abruptly to lake Placid, but to the north-
east it is prolonged in a high ridge called Wilmington mountain, that reaches
3,500 feet. There is one pass at an altitude of 2,300 feet with a road running
through it from Wilmington to Franklin Falls. The draimage from the
western side of the range flows into the Saranac river.

Series I and 17, with my interpretation of the gneissoid rocks, are lacking
in the town, but I appreciate that the northerly extension of the Wilmington
range may be, perhaps, with fuller study, in part, at least, classed as such.
Professor Cushing has considered the extension over the town line as
belonging to the gneisses. The mineralogy of the rocks gathered by me is
siven under the next topic. Series II may reach a short distance across the
line on the southeast.

Series ITT, All along the easterly portion the rocks are green anortho-
sites or gabbro. No. 20 is a coarse pegmatite with pyrrhotite, and forms a
limited occurrence in the other massive rocks. At No. 24 the usual anortho-
site crops out, showing the familiar crushed structure. At No. 27 the rock
becomes more basic and like the gabbros and at No, 28 a granulitic phase was
met, much the same as those described in my former report, page 469, from
the Weston iron mines near Keene. The mass of Sentinel mountain has only
been traversed by me around its base on the northerly extension. In Keene,
however, we have crossed it finding anorthosite all the way. On the
northwest side too we have studied its foot along the West Branch. Though
often gneissoid, it uniformly exhibits, so far as seen, the minerals of the

gabbros. :

y,

PLATE ¥

Sek ey KVR x
TK SOOM KYO

HR PRR RIO
CS eGR.

; INK XX RR RLY)

0 | Oy KY YY

PRL ons NER 4 RX SARIN) x
RRS ARONA AXXO
AI INK AN ROA ARES
I ANSON RR SRR AN NORA
NAO MR SCN Oy py KX)
LOMO SSSR
EOIN ORO CYL SEIU LOA YY
OR OAR OL Ra SERA)
Ox BRT IO ROAR XN ERAN OY)
MIO EL OREN MN)
OK AYO NIRS QROOXK YX)
OER IGOR OX MOSK KSI
NN
QOMOMONE MMO MAaElm COMMONOOe\
i a Mann
WOH AR OR ON KK KRIS

GRA RAN XAT XY
MAX ORAR OXY ROX IX KK
QI MEX RK NA RAK RT KK KAY
HRN KK IK ROK WRENN KN

OOO AAI ABER OAK YY
Go ONO SANSOM MOMMNONG
SISSIES NR
FERREIRA
LAK eee \K) POX ORY M
ser RL XR SAR) nN Xwiei
OSL RE

KKK WA

vegans XY SAX \% (\ XX HOY xx XX
x OOP RYN in ett ea x
HORAK K KOR
ENON
RON RRR
i X XK WY BNR
OA AERA
( ON ISEAROR ORY
OXY)

e,

CIAL

GLA‘

CAMBRIAN LOWER SILURIAN

GABBRO

CRYSTALLINE /ANORTHOSITE

“GNEISS”

GRAVELS ETC.

CALCIF
CHAZY
TRENTON

Se SS as ee
ro fe GF e€Ter)
bees es L

POTSDAM SAND

SCALE OF MILES

LIMESTONE
AND BLACK SCHISTS

GNEISSOID

°

GEOLOGIC MAP OF WILMINGTON TOWNSHIP.

ANORTHOSITE OR GABBRO

plate?

nail

.

| paengny

dx teysuete,

ae |
nom repuaet

- wr

Ee

*

3 ‘ fe ( Pi Y x KAM . f, ‘ > i ay i

€ re ie:
J , . *) 452)

¢, i

ntane

ny for
i
| the uorthariy

BY RY 5 ; by . y aX

ol \ ne) $,¢ x % rare | a : M) ;

a Ap) .. Py é J ¥, ee ‘he } “* ? ; ‘S
EER NOS CASRN URANO

-

tiatigxd aconetiirey ”

Rofeat) bot ¥
i

|

ahr busch aii NG,
; Yonder ek

7 hs

Lar

|
‘

So
5 planet 33

t ih fn
AUS ie Pia se

STASI
tera

Rod? Ober
>
~—

a 2
SB ,8, E's »

ira

Oe Fae tL) 9 “2 L
2 OKC y ee W at $0.6; ae tie
* ; if wae Cnr ae ee 7 he iy

Adel, hese .éxiealty

SDR OSO EER BOR OV YK i
Bax sae} bs V7 Me 0 ite Ny K

‘3. f CH)

ON ahedee | me

Rake AK ee i Oe
we A

9,

f O

¢ x POY?
% ER XY
COO $ re WX x XR

aca *
Faye
Re
Pat hes |

if

ke
Shs
ssh

‘6 x
eee
¥ F . oN i
SAY EY
ie < RS ann
ee ie “S, ? wh

.

iy ¥

JA 30

ee.
‘

Kemp—-Grotoay oF Essex County. 587

The ridge of Wilmington mountain in the northerly portion has been
traversed at No. 43b. The rock is gneissoid with the usual minerals of the
gabbros. In the pass at No. 44, the gneissoid structure also holds, and in
thin section the rock shows labradorite, hypersthene, garnet and brown horn-
blende. At No. 46 it is chiefly labradorite.

The rock of Whiteface mountain is quite different from the usual types
elsewhere in the mountains. It is a markedly white rock through which are
distributed dark bunches of ferro-magnesian silicates up to half an inch or
more across. It looks like a light granite. It is not strongly gneissoid,
although faint lamination is distinctly visible. Under the microscope it
exhibits plagioclase, brown hornblende, pale lavender augite, magnetite,
presumably titaniferous, and titanite. Pegmatite veins, strongly quartzose
run through it at the summit. The rock on the way up from Wilmington, at
No. 47a, is strongly laminated, with a nearly north and south strike. On the
trail down to French’s, at No. 49, 1s a very gneissoid type, with a true strike
of N: 25° E.

The rock under the microscope is chiefly untwinned but very coarsely
microperthitic feldspar with an extinction on the cleavage, up to seven
degrees, so that it appears to be orthoclase. The inclusions are spindle-
shaped, but curve and are irregular. Their general alignment ranges up to
twenty-five degrees with the line of extinction of the enclosing feldspar. The
other minerals are diallage and a few shreds of quartz. The rock is very
puzzling, exhibiting as it does the characters of both the gneisses and gabbros.
Future and more thorough exploration may lead to the determination of some
of this great ridge on its northwesterly side as belonging to the series of
gneisses. It needs more exploration, but as it is a heavily wooded district and
remote from settlements, it is less accessible than many other districts. I
have provisionally colored it as belonging to Series III, as such is my
opinion from observations thus far made. The same rock that forms the
peak of Whiteface mountain extends well down to the shores of lake Placid,
and further along the ridge to the northeast in the pass, the rocks, as already
stated, have the mineralogy of the gabbros.

After leaving Station 49 no more actual outcrops were crossed by the
trail which passes down through thick woods. All the boulders that were
met, and some could not have been far from their parent ledges were gneissoid
rocks of the mineralogy of the gabbros. But soon after leaving No. 49, the
trail passed into St. Armand.

Series IV entirely fails in Wilmington.

588 Report oF THE STATE GrOLOGIST.

Series V. At the High Falls of the West Branch, near the North Elba
line, a trap dike of eight or nine feet in width becomes the directing agent of
the stream and explains the deep and narrow gorge by its easy decay and
erosion. Immediately associated with it is much coarser crystalline red
granite, precisely similar to the association of the dike and granite at the falls
and gorge near Keene Center, as described in my former report, p. 468. The
granite is older than the dike, for inclusions of its red aggregates of quartz
and orthoclase are frequent in the trap.

Series VI, 'The sands and gravels of the glacial and post-glacial times
are strongly developed in the northeastern corner. They lie well up the
valley of the West Branch. The most abundant by far are in the nature of
water-sorted materials, fine sands and gravel.

Mines and Quarries. There is an abandoned prospect for iron ore just
west of Wilmington, called the Weston mine. It was never a serious producer,
but attracted attention im connection with the bloomery that formerly was
operated in Wilmington village. The associations would indicate a
titaniferous ore. The existence of a pegmatitic development of anorthosite
with some pyrrhotite near the little post office of Hazleton, has been
mentioned under No, 20. The samples shown me were only of mineralogic
interest, although of course the general geologic relations in wall rocks of
the gabbro family, suggests the presence of nickel and cobalt, but experience
in the norian rocks of the Adirondacks and Canada to date has only developed

titaniferous magnetites as the ores present.

St. Armand.

In my previous report a short sketch of the northwestern corner of this
town was given and it was shown to be of the typical gneisses of Series L.
In September, 1895, I was able to gather some further details, and have
redrawn the old map so as to include them. Nevertheless, the lack of time
and means, the rainy weather and the pressure I felt upon me to make a
reconnaissance of the southern tier of towns of the county, prevented the trips
into the wilderness along the southern boundary of the town that I expected
to carry out. Since the field work of 18938, the lake Placid sheet of the United
States Geological Survey has appeared and has rendered available a map of
the eastern half. .

Zopography. St. Armand lies along the Saranac river, which cuts it on

the diagonal. The northeastern corner is covered with sand and gravel and

GLACIAL
GRAVELS ETC.

LURIAN

SS

OX <5 ay
a

Up

Kw
Nicaea
XXX

SO

“= AW AW! LA
RARER IN
OX
Maas

CAMBRIAN LOWER 5I

Q
Pas
<
v
=
3
5
a.

y)
uJ
_
2
Le
fo)
uw
<
O
y)

ISG
GABBRO

EX SO5GH

PLATE
WKY
A,

AS
VO:
A
Poet \’

<
SSS O5 2s
Sees Se
oSOSSS BOSSSSSSOS
SESS
ANORTHOSITE

LIMESTONE
AND BLACK SCHISTS

CSS
vee se
CRYSTALLINE

aff 8
in Ae
zeq 2h
OFF $k

°
GEOLOGIC MAP OF ST. ARMAND TOWNSHIP,

JAANORTHOSITE’ on GABBRO

Mian:
f*4 4 *oR» .

Nor
a,

x?

A hr
AY

Se he ;
tag ge On pe eee =

Ate To ets ws GUA qise2
co} Se Ld Ue :

ret “ory
cae ts : mo
- : ~e

we

© OTD G4SVARO “any Gees Ae A
car Manet ER GREGGAD AO STIZONTROMA

Kemp-——Grotocy or Essex County. ; 589

is of mild relief. Along the east and south there are the spurs of Mount
Whiteface, and further west the ridge of Moose Pond mountain, all forming
a practically unbroken wilderness. The mapping of this section is tentative
and is based on the inference that the rocks in the edges of these ridges as
met in North Elba on the south and Whiteface on the east continue toward
the north, but where the line, if indeed it can be made out, between the rocks
of Series I and Series III is to be drawn, must be investigated later. A
high ridge bounds the Saranac river on the west, south of Bloomingdale,
and another appears north of the river and east of this town.

Series I. At No. 51a there is a red orthoclase gneiss. At Nos. 52a and
52 the gneiss is dark green, and is the same as No. 2 of the Jay map. Under
the microscope it exhibits microperthitic orthoclase, a little plagioclase, and
some almost opaque hornblende. Zircons are also not lacking. At the
bridge over the Saranac there is an excellent exposure (No, 52). Outside the
township, in Franklin county, the gneiss rocks continue beyond Franklin
Falls, and two miles down the river there is a goodly ledge of the familiar
white, crystalline limestone, charged with pyroxenes, titanites, bunches of
hornblende, pyroxene and quartz. The dark hornblendic schists that always
accompany the limestone, are also well developed. All these indicate that
the anorthosites and gabbros, so far as present, lie south of the Saranac river
in this town, although we know that they exist near St. Regis lake to the
west of the line of Essex county. The strike of the gneisses is mostly north-
east, but east and west and northwest strikes are known.

Series II is not met within the limits of the town, although, as stated
above under Series I, it does appear about three miles north of the line.

Series III. The area covered by these rocks is mapped on an inferential
basis from observations on the prolongation of the ridges south and southeast.
While actual study of the rocks ¢7 situ may modify this, I consider the
inference as worthy of confidence in the present state of our knowledge.

Series IV is entirely lacking.

Series V. No dikes were noted in the town itself, but just over the
border at Franklin Falls one appears in the side of the road near the hotel,
with a northeast strike. It is a dark trap, presumably diabase.

Series VI. The modified drift is widely spread in the less elevated
districts. In the northeastern corner it covers several square miles so that no
outcrops are available. Level meadows suggest at times former ponds or
lakes, and the extended one near Bloomingdale station, outside the county,
was referred to in my former report, page 472.

590 Report oF THE State GEOLOGIST.

North Hudson.

Topography. North Hudson is one of the largest townships in the
county. It les just south of the principal peaks of the Adirondacks, but its
line includes the summit of Mount Dix, 4,842 feet above tide, the sixth in
altitude of the high peaks. McComb mountain reaches 4,425 feet but the
others are all below 4,000, and only one approximates this. The ridges have a
marked trend, a little east of north, and all the valleys and larger watercourses
show the same characteristic. The town contains several large and fairly open
valleys. On the northeast it is marked by rather low hills, 500 feet or so
above the upper waters of Schroon river which, near Deadwater pond, are
about one thousand feet above tide. ‘The same character continues along the
east border. The Schroon river flows with a rather sluggish current
southwest across this portion, the total fall in twelve or fifteen miles being
about 200 feet. The valley is a fairly open one, is filled in with sand, and the
highway is nearly a dead level, often for long stretches. West of the Schroon
river the country is much more rugged and elevated and is practically
uninhabited except for the sparsely distributed houses along the road to
Newcomb.

Immediately west of the Schroon river, Saunders mountain, Old
Far and Little Far, Niagara mountain, Nippletop and Wyman hill make a
considerable rampart, that is broken where the “ Branch” comes in from the
west to the Schroon river, making thus one of the few east and west streams
of the region.

The next great ridge to the west containing Spotted mountain,
McComb and Dix, is separated from the ridge just mentioned, chiefly by
Niagara brook, which flows along the excessively steep westerly slope of
Niagara mountain, taking its water exclusively from the west side of
the valley. Further south comes in the “ Blue Ridge,” whose culmination is
Hoffman mountain, just over the line in Schroon. West of McComb
lies the valley of Elk lake, a wide and somewhat swampy one with the lake
in the middle. It forms the source of the “ Branch.” West of this lies Boreas
mountain, nearly 4,000 feet (8,815) at its culmination, which makes the
watershed between the tributaries of the Schroon and the Boreas rivers, and
between the Schroon river and the East Branch of the Ausable river. The
headwaters of the Ausable and Boreas rivers are in another broad northeast
and southwest valley that is marked by wet meadows and lakes. In the
northwest corner of the town are Cheney Cobble mountain, 3,673 feet, and the
slopes of Allen mountain, that culminate just over the border at 4,345 feet.

~S

| XXX)
GWMOLOSONNnnnns
Awana nanauennne
ANY Se

ae
ROSSA
x SSSI
KAA XX 7 Ci A
WS SSas ers ies NX Un oneniins

4
Ds

Cry

yk
OO

XK
CK

°
rt 2

GRAVELS ETC.

GLACIAL

90 %6 ©
le
°

\
\

ae Av , ,
PIS: y teh lt 4 Y
ONG YE ye;

Y

(j

23 CALCIF

OIC) CHAZY
L__l_| +RenToNn

$s
~

im

00%

Wi
ie

y,

See ees Beas cee
=] Loe a ¢
Care es
eee

POTSDAM SAND

SCALE OF MILES

()
WY
ine

44
Ms Po Goce!

XA

i

X)

al
\
CAMBRIAN LOWER SILURIAN

io ~ ON
MxKY’
WY ‘
‘\ ve
x:
%

(XX)

CX)

6G
COE ONG
OOK

{xX
WV
Ks

AX KY
¢,
.

?
RN

vi

vas

4,

7,

00%
OX
XX)
Bes
BOK

©,
Hy) XY

\)
Xr) Y,

aA:

Xx

GABBRO

()
)
iy

<a
2S
CSC SO4

<>

SoS

|
Le

SJ
: ‘
HUDSON TOWNSHIP.

z>
es

ANORTHOSITE
~<SO

i
stae
KS

oe
—
NST SSN |

%

Waueunonnnne-

Me auennnenes

LO ik

Beeh ROMY RNA

XK WOSaaXys

Ns ye Bs Pens
ee

PLATE VI

A

is
CK

MK

rite

o, .
16s

LIMESTONE
AND BLACK SCHISTS
GEOLOGIC MAP OF NORTH

CRYSTALLINE

LOS SONS SRB
KR MW iN eh X HS OK
LER Mei
CMOS SS SISSON
G99 ™ XL EAE
OX XX XK KA KAA) MAY) =
DT SN SIMEON SNOSS A mel?
MNO Tops a 4 Z

RANA
MME i
w ey cignen ie
SOP RK MO AOAC RACK KIX
SEY AMS (x) i
y “4 SAKA Xx XX Pw
YY
f\

2X Kaa)
ANORTHOSITE OR GABBRO

SES

i)

GNEISSOID

, *
SOXXX WY
Ni ys WAX
Ry SONMiione OG 4%
Veen PLANE)
CX
KX

, OXY
AEX

x. . () ™) (Kp
A RN OXY f
» as
YY?

XA
i ONY
Sone
Oe

Me

OXXKKK
XY
SO

he

Y LKX)
¢ XX)
0

6 WK)
in Of K AK
X BSCS
OPO RAR Wn

Garr
Very WW

SONOS Be Asin

BOOK LY he ROA

‘ Canes SOKA
ONG, XK XY ‘\ (

KX AX MX MN RIAA XY) XXKN
ONION ICAI A NR
|

WOKS
ETI

44

)
(X ON (\

WW

ce x
Me ays

. tf

-< — ‘ ‘ a : .

i uy = é = e

u ~ 5 - -
= rit =
y “ e.
'
de 7 q 4
#0 “

e- . Ba 4
= “ a 3

da : _
o ‘ H > *

'
i -
7 *
~

Kemp—Gronocy oF Essex County. 591

The Boreas river passes out of the southwest corner of the town into
Minerva, with various minor tributaries heading in hills of moderate
elevation.

Geology. So far as I have explored North Hudson, only the rocks of
Series III have been met. I have crossed the northwestern corner, coming
down from Marcy to the Upper Ausable lake. All the rock visible was
anorthosite. In the northeast and east all the roads on the map have been
traversed and the anorthosites, related gneissoid types and gabbros have alone
been met, but it is quite possible that the gneisses of Series I may be present
in the northeast corner. No. 60, near Underwood, is crushed anorthosite; No.
61 is massive gabbro; No. 63 is also massive but is very finely crystalline ; No.
64, near Root’s hotel, is typical crushed anorthosite. All along the highway
that comes in at Chafey’s from the east, is Series III, an extension of the
ereat area that forms the prominent knob of Harris hill just over the border
in Moriah, and Moose Pond mountain in Crown Point. The road that comes
in to the main highway, just south of No. 64, from Johnson’s pond, traverses
anorthosite all the way. At No. 108a, where the highway along the Schroon
river crosses the town line, there is an outcrop of dark typical gabbro.

On the highway that crosses the southern half of the town from Root’s
hotel to Newcomb, the rocks are anorthosites and gabbros more or less
eneissoid. Gneissoid rocks of the same type are met on the town line where
the trail in the southwest corner crosses the town line. I have reached that
point coming up from the south in Schroon. The valleys in the interior
of the town have not been visited, but as anorthosites and their related rocks
are found on the north in Keene and to the northwest in Newcomb, it is
unlikely that any other series will be met.*

Series I and JT are lacking so far as we yet know.

Series IIT covers the town so far as our present knowledge goes. See
above under Geology.

Series IV is lacking, but it is extremely probable that it formerly
existed in the Schroon river valley, as a small outlier is still preserved at
Schroon Lake post office.+

Series V. No dikes were observed, but they doubtless exist.

Series VI. The usual sands and gravels are present all along the
Schroon river and at times form level stretches of noticeable extent. They
are even abundant enough to be quite seriously drifted by the winds in one

* They have since been thoroughly traversed, and only Series III has been found.
+ A small area of Potsdam sandstone has been found in subsequent field-work, about a mile north of Chafey’s,

592 Reporr or tHE Stare GEOL GIst.

or two localities. To what depth they fill the valley is uncertain, for the
Schroon river has not excavated them to bed rock. Lakes or estuaries must
have existed after or during the wane of the ice-sheet in order to have made

possible the abundant deltas.

Schroon.

Topography. Schroon is a township lying along the southern limit of the
high peaks and partaking both of their topography and of that of the more
open country further south. It contains the northern half of Schroon
lake and all of Paradox lake, the largest two in Essex county. The
town is cut into two nearly equal portions along a north and south line
by Schroon river and lake. The valley of Paradox lake, running east and
west, cuts off the northern third of the eastern half. It is a region of
moderate elevations formed by the outlying anorthosite spurs of the great
Moose mountain ridge of Crown Point and North Hudson. The highest
summits reach 1,700 feet. Paradox lake lies in an irregular east and west
valley, with its surface 820 feet A. T. To the south is a wilderness of
moderate hills with one very prominent peak, Pharaoh, 2,557 feet, that is the
chief land mark of all this region. Lakes and swampy valleys lie in among
the hills. Passing along the southern line the same topography continues to
Schroon lake, which is 807 feet A. T. The altitudes therefore of Paradox
and Schroon lakes differ but slightly, and in high water it is reported that
Schroon lake rises so much faster than Paradox that the drainage is temporarily
reversed—whence the name “ Paradox.” It is quite evident that they were
one continuous body of water in recent times and that the Schroon river has
built up an extensive sandy delta that has cut them apart. Its course over
sands and gravels for ten miles or more to the north has furnished it with
abundant sediment in the immediate geologic past. West of Schroon lake,
the southern line cuts Green hill, which reaches the respectable altitude of
2,227 feet. Passing along the zig-zag boundary to the north and west, deep
valleys and fairly high hills prevail. Near the northwest corner, Hayes
mountain just west of Bailey pond is 2,822 feet. The northern boundary
crosses a series of high ridges with a marked north and south trend and
with narrow valleys or notches between. Washburn ridge culminates at
2,938 feet, Texas ridge at 3,212 feet, and Hoffman mountain, the nucleus of
them all, at 8,715 feet, the highest in the township. This region extends as an
unbroken wilderness until the valley of the Schroon is again met. The

central part of the town is fairly open and quite generally settled. Beech hill

PLA

3 Yo SLY
WINNING
cast
RN We
OEE
BERL ORXNRY
ee os. uy
Vas, EEL
Pa
RAXK RR Can
x :
BO aie
A XSRKRRR AR NO
DEB AAAX RENE
FC ees
CR NR
LS ES
AX KOEN OE
REAR AAR
RXR AERO KRY
I RIA GRAIN AN ON
PERRIER XR RR OR RNIOE
RRR RIKKI A
RSH
OOK RSA KR KAY OO eT
a
ORY AAA
KAKA RRR eRe
XR ANON :
Wraiarenntarancaracrrncancnta
YAR ERRNO ERR N
¢ XK ¢
ea
OG
AX y, \ oa"
RUAN RRR RON
iNatunleitirgurscetatare canary oes:
Mr sieartartonreirars serum vac neds
RENAN AORN RN
RRR RRR
RAEN a esae
Wire SeonannenscPe
RNR RN RE ZZ
QR REA. ZZ
ies cal

7

GLACIAL.
unica GRAVELS ETG.

CALCIF
CHAZY

a Cees |
aera
SS me |

CAMBRIAN LOWER SILURIAN
saat
ree
Fale)

POTSDAM SAND

SCALE OF MILES

GABBRO

x

ANORTHOSITE

LIMESTONE
AND BLACK SCHISTS

CRYSTALLINE

GNEISS
IARNN

GNEISSOID

CS)

SE
ANORTHOSITE OR GABBRO

<>

Sz
cS

3
GEOLOGIC MAP OF SCHROON TOWNSHIP.

Lu
°

te ‘
tie
* - ™
fi ®ve
* Rea |
' y dail
4
rr y “4
¥ ‘9 i
—
a i
td jo
* "4
7 ‘
- 2
f
~
ri
f Lf
4 n t
r
1 ; .
ve
7 ‘
. ; f
‘a
ro
}
= *
F ‘ 3
; Mi
‘
"
; 4;
| A al
r
“
= i
‘
{
. a
)
es :
* &
“=a
—
“ ‘A
|
: 4
? = j
‘
: +
,
Cail ¢
4 4
: 1 ay :
Y / fo
t “4 ;
ab
t ' ‘ J
7 ae ‘
- ";
=
w, “J
/ ye
dea Mx td
| i 5
‘ae 7
a 1 See
ry 7 , er
4, , )
} {
.

Krmp—Grontocy or Essex County. 593
at 2,203 feet is the culminating point of the largest clump of hills, but
farms extend almost to its summit. The drainage of the western part of the
town is mainly through Trout brook into the Schroon river in Warren
county to the south. The exceptional interest that attaches to the topo-
graphic relations of the Schroon lake basin are later commented on.

Geology. The northern portion of the town is formed by Series III,
but almost all the remainder, except for outhers of gabbro, consists of the
eneisses and crystalline limestones of Series I and II. A small but
extremely significant remnant of Calciferous cherty limestone covers a few
acres at Schroon Lake post. office.

Series I. As shown by the map, the southern portion of the town to
the extent of more than half its area is formed in largest part of gneisses.
The gneisses vary somewhat among themselves, but a light colored, strongly-
laminated one, shown by the microscope to consist of quartz, microperthitic
orthoclase, prominent garnets and a little hornblende, is a very prominent
type. It is the principal rock around Schroon lake, and in the country to
the southeast around Mount Pharaoh and Pharaoh lake. Hornblendic
varieties also appear that are darker than this one, and still different varieties
as noted in the detailed itinerary that follows,

The valley of Paradox lake is bounded on the south by the limestones
of Series II, but on the eastern border of the town, at Nos. 100 and 101, is
the Schofield ore-body, whose walls are a massive gneiss, precisely like that
which contains the ore at Hammondville. It is little else than plagioclase
feldspar and quartz. A few magnetite grains appear, but the rock is a very
pure aggregate of the two minerals mentioned, right up to the ore. The hills
and ridges in this region are very generally gneiss, while the lower lying slopes
and depressions are limestone. Along the highway to Crane pond, No. 97 is
a coarse gneiss of interlaminated flat lenses of quartz and orthoclase, which
have evidently been rolled out under dynamic stresses. In the slides, strained
or crushed crystals are abundant. Very little hornblende is present. Along
the east shore of Schroon lake, the rock is a coarse quartzose gneiss, at times
with mica, again with hornblende, and often with garnets, while along the
highway which lies in part in Warren county, it is much the same, and is the
garnetiferous variety cited at the outset. The same rock makes up the mass
of Mt. Pharaoh. A fine illustration of a brecciated gneiss was met at No. 69
on Pharaoh lake. This light garnetiferous gneiss leaves a strong impression
on the observer that it is clastic in origin, although precise evidence is ditt-

cult to obtain.
38

594 Report or tHe Strate GEo.ocist.

The gneisses form the western lake shore, with intervals (Nos. 76a, 77).
No. 78 is a light grey vaniety like ‘that of the western shore, but No. 76 and 79
are darker, full of plagioclase, with brown hornblende, and in No. 76 diallage,
so that the mineralogy suggests an altered igneous rock. The gneisses
continue across the hills on the south. At No. 109, on the southwest,
quartz-hornblende-gneiss 1s met.

On the highway running west from Schroon lake post office, at No. 83,
is a quartz-hornblende-gneiss, and at No. 82 a basic hornblendic variety.
Outcrops are few along the road to the west, but the gneisses and limestones
occur just over the border in Minerva, along this general line. Particular
interest attaches to these relations because just to the north the spurs of
Hoffman mountain begin to rise and shade from gneissoid gabbros into the
massive anorthosites, so that the highway is not far from the boundary
between the two.

Series II. The crystalline limestones are quite widespread and of con-
siderable areal importance. As always, they favor the depressions. Along
the south side of Paradox lake they are strongly developed. At No. 98b, is a
high ledge with a good-sized cave extending into it. The limestones reach
up into the valley to the northeastern portion of the town, and are prolonged
into Crown Point, as shown on the map of that town already published. In
the valley of Alder brook, that is the outlet of Crane pond, the limestones are
abundant all along the highway, and with them are the usual black schists.
The limestones appear again at Nos. 76a and 77, on the west shore of Schroon
lake. They were not met elsewhere, although abundantly developed in
Minerva.

The limestones are white, coarsely crystalline and graphitic. They
seldom show any large cross-section, say twenty-five to fifty feet, without
bunches and knobs of dark silicates, or scattered irregular bits of pyrrhotite,
hornblende, pyroxene, flakes of phlogopite, ete.

Series ITT, The anorthosites and gabbros constitute the northern portion
of the town and rather more than one-third of its area, They are prevailingly
eneissoid, and as the areas of the gneisses of Series I are approached, they
become very strongly so, almost to the extent of schistosity. This tends to
decrease in the interior hills, and at No. 95 quite coarsely massive varieties
are attainable, All over the adjacent areas on the south are huge boulders,
often as large as a small house, of the Hght bluish anorthosite, that has
come from the inner hills. At or near No. 87a, I paced one that was roughly

oval, 30x 20 feet, and that projected six feet above the turf, with an unknown

ihe

Kemp—Groxiocy or Essex Counry. 595

extent below ground. Others often stand in full exposure, 10x20 feet
in dimensions. The district is the most prolific in them of any traversed
by me.

Aloug the highway in the northeast corner, gneissoid anorthosites are met
at No. 108 and alternating with gabbros (No. 104) they continue along that
road over to the valley of the Schroon. On the highway in the Schroon
valley, massive gabbro is met at No. 103a, and massive anorthosite at No. 105.
Gneissoid anorthosite forms the north shore of Paradox lake at No. 106a and
No. 106b, but quartz gneiss outcrops at No. 106. On the west side of the
road up the Schroon valley, the anorthosites are met in the hills and have
gneissoid laminations more or less distinctly developed. In the foothills to
the north of Rogers pond, thinly laminated basic gneisses, manifestly derived
from gabbros, are first traversed and only yield to the more massive forms in
the interior peaks. The region where Nos. 85, 86 and 86a appear is a very
difficult one to cross, as there are no trails and as it has been recently burned
over. On the northwest, gneissoid anorthosites again appear at No. 88, and
over to the north of Bailey’s pond, with varying accessions of dark silicates,
they continue to the North Hudson line.

The exposures and float masses of the rocks of Series III in this
town have given some of the most interesting data regarding the dynamic
metamorphism of these rocks that have been met in the mountains. Perfectly
massive varieties were collected, consisting of a coarse aggregate of green
labradorite, with perhaps a stray hypersthene, augite or hornblende crystal and
a garnet or two. Crushed rims around the crystals first manifest themselves
and increase gradually until the rock consists of nucleal fragments embedded
in a white pulp of comminuted feldspar. Such varieties I have called pulp
anorthosites. Apparently these have resulted largely from crushing strains
without much shearing. When the latter is superadded, the crushed materials
are dragged out ito the laminations of a gneiss, with the nucleal crystals left
as lenticular “eyes” around which the laminae pass. Abundance of dark
silicates accentuate the laminations, and the development of garnets makes
them much more prominent. The formation of this latter mineral is a
question deserving much careful study and chemical analysis. It is a
remarkably common and characteristic mineral all through the mountains and
is present in all the older rocks, but especially in those of Series III. It
seems to result from the pyroxenic constituent and also to develop in purely
feldspathic rocks, and in these it may be in fairly regular dodecahedra three-
fourths of an inch in diameter. It-is a deep rich red in the rocks of Series

596 Report oF THE Strate GEoLoGIst.

‘

III, but is notably paler in those of Series I and II. I expect to give the
subject of its formation detailed investigation in the future, as opportunities
occur.

In distinction from the more feldspathic members of Series III, of which
special mention has been given above, often under the name anorthosite,
attention should be directed to the dark basic gabbros and their meta-
morphism. Although the latter are best exhibited in Moriah township, on
lake Champlain, just north of Port Henry, they are also, to a less degree,
shown in Schroon. The dark gabbros often contain olivine, and are a
plutonic rock, rich in pyroxene, brown hornblende, titaniferous magnetite,
and a dark green plagioclase that tends to develop somewhat lath-shaped
crystals and, in many specimens, to suggest the diabase type of texture.
Excellent exposures occur along the highways on the northeast at Nos, 104
and 108a. The last named is a large ledge, perfectly fresh and extensively
blasted out on account of the passage of the road. In the extreme southeast,
on the shore of Pharaoh pond, is a dike twenty-five feet wide, of well-marked
gabbro, far out from any visible parent mass, and in walls of light grey
quartzose gneiss. Again, west of Schroon Lake post office, on the lane
leading out toward Rogers pond, at No. 84, is a fine outcrop of coarse dark
olivine gabbro.

These massive gabbros, when subjected to shearing stresses, develop
dark hornblendic schists, and this change can be shown even in the limited
exposure of the rather narrow dike on Pharaoh pond. The feldspar is
crushed, and the dark silicates are dragged out into thin laminae. Even the
massive types have seldom escaped the production of reaction rims_ of
garnets that mark the boundaries between the feldspars and the dark silicates
or ores, almost never allowing the former to come into actual contact with
the latter. Hypersthene, brown hornblende and biotite also enter into the
rims, especially where they surround magnetite, but garnet is much the
commonest and most noticeable of them all.

Series IV. Much the most interesting and significant of all the
exposures in Schroon township is that embracing a few acres of what I take
to be the Calciferous formation. The rock is a grey, cherty limestone or
dolomite. It extends along the shore on both sides of the steamboat dock at
Schroon Lake post office, and has a total outcrop of about 400 yards. Rogers
brook falls over a ledge of it and affords the best and most extended cross-
section. The strike is by the magnetic compass N. 60° E., and the dip is 25°

N. W.. Referred to the true meridian this would be 10 to 12° more to the

Kremp—Groitoey or Essex County. 597

eastward. Roughly but carefully measured, the total thickness exposed above
the lake water is about seventy-five feet. Streaks of chert run through the
ledge, and coaly or asphaltic material appears in the cracks. Calcite pockets
are not lacking but, although I searched carefully over the ledges, I was
unable to find definite remains of organisms. Thin sections of the chert
merely exhibit a brown, nearly isotropic base with numerous rhombohedra
of calcite or dolomite scattered through it. A few opaque ones are
apparently limonite residues after original siderite. This outcrop was noted
by Charles E. Hall in his report on the Laurentian Iron-Ore mines of the
Adirondacks (Thirty-second Annual Report New York State Cabinet, p. 139),
who speaks of it as Chazy and as containing fossils. Fossils sufficiently well
preserved would, of course, settle the stratigraphy at once, and I feel the
greatest hesitation in speaking of the ledges as Calciferous in opposition
to the earlier record. The resemblance is so close, however, to the
cherty magnesian limestones that are undoubtedly Calciferous and non-
fossiliferous on lake Champlain (as for stance just north of Port Henry, and
again just north of Crown Pomt on the Delaware and Hudson railway), and
the probability of Calciferous in this outlying district resting on Potsdam is
so great, that I leave the determination as stated, being ready to recall it if
the evidence of fossils should be against it.

The interest of the exposure lies in the fact that it is the remotest
outer yet found of the Palaeozoic sediments in the mountains. The
nearest outcrop is the little area of Potsdam sandstone, distant at least
ten miles in a direct line in the Putnam’s pond valley of Ticonderoga
which, however, drains north through Penfield’s pond in Crown Point
to lake Champlain, The actual divide at the head-waters is insignificant.
Down the Schroon and Hudson valleys the nearest exposure recorded is at
Hadley, about forty miles away. There is little doubt, however, that the
Hadley tongue formerly set back up the Hudson and Schroon valleys,
and that this little outlier is the only remnant, so far as we now know,
that is left. Hadley is given by the railway (see Macfarlane’s Geological
Railway Guide, Second Edition, p. 118) at 606 feet, and Schroon lake
has lately been determined by the United States Geological Survey at 807
feet, so that the rise is now about 200 feet. The interesting point is
whether these modern valleys were depressions and embayments up which
the oceans set in Cambrian and Ordovician time; or whether the early
Palaeozoic strata spread all across the crystallines and have only been

preserved in small in-faulted blocks, whose faulting is relatively modern.

598 Report OF THE STATE GEOLOGIST.

The former has been the case with the lake Champlain basin and
apparently with its arm up through Crown Poimt and Penfield’s pond
into western Ticonderoga, along the easterly branch of Putnam’s brook (see
map of Ticonderoga, Report of the State Geologist of New York for 1893,
p. 452); with the lake George basin and its arm up through the Trout Brook .
valley in Ticonderoga (see last reference), and in the Hudson - Schroon
valley, we have doubtless still preserved for us the old Cambrian-Ordoyician
topography. It is furthermore a curious fact that the strike of all these out-
hers is northeast, and the dip 1s also low to the northwest. It is remarkable
that the same strike and dip hold good for the embayments of these rocks all
along the west shore of lake Champlain, in Essex county, and notwithstanding
the minor faulting we cannot well avoid inferring that there has been con-
siderable tilting in which the county to the east and southeast has risen.
The Green mountain upheaval may in part account for this, but the Schroon
outlier is a long way into the Adirondacks to have felt its effects, when it
produced such shght tilting along lake Champlain itself, only twenty miles
away from the principal elevation. If we assume anticlinal folds instead of
faults, it is extraordinary that the eastern limbs should be eroded while the
western remain. Tilting in blocks with fault lines approximately parallel
to the present valleys, is more likely to be the true explanation.*

It is also worthy of remark that the Schroon valley is a base-leveled one,
or nearly so, except as concerns side tributaries. The Schroon itself is a very
sluggish stream for a mountainous one, and the fall is very slight, as was
noted above under North Hudson, from its source to Schroon lake. Such
obstructions as 1t is now at work upon are chiefly glacial deposits. The great
geologic age of the valley no doubt accounts for this sluggishness and the
question may be raised if other slow streams, not evidently held in abeyance
by glacial deposits, may not be explained in the same way.

Series V. Several dikes have been noted. The point on Pharaoh pond,
where No. 70 is located, is well provided with them, as the accompanying
sketch (Figure 1) shows. The laminations of the gneiss run straight across
the strike of the dikes. The dikes have also proved an easier prey to the
weathering effects than has the gneiss and the retreat of the shore along their
lines has in part at least caused the points. The dikes cut pegmatite veins,
and in one case a small dike cuts a larger one. The occurrence of these little

scraps of igneous rock in doubly terminated fissures and running like veinlets

* Since the above was written, topographic maps of this area have been issued by the United States Geological Survey, and
based on these, the writer has discussed this question at greater length in the ‘‘ Bulletin of the Geological Society of America,”
Vol. VIII.. p. 408, Plate 51.

-_~
-_-~
—

GroLocy or Essex County. 5

Kemp

all through the gneiss is remarkable. We can only infer that the intrusion
of the larger ones extensively shattered the walls and that the molten trap
oozed into every notable crevice. The rock is a diabase. The presence of
the gabbro across the lake at No. 73 may be remarked, but I see no reason
to connect the two. A very similar group of little dikes was also met west
of Schroon Lake post office at No, 83. The accompanying sketch (Figure 2)
illustrates their relations. The exposure was only a small one, eight or ten
feet square, and the tiny dikes were faulted in an interesting way, as shown
in the figure. ‘The smallest of these was doubtless originally continuous.

PHARAOH

Ww

OD CALE 50FT.
ee ae |

FIGuRE 1,

Series VI. The glacial drift is very generally present, and, as already
remarked under Series III, enormous boulders are of great abundance just
south from the mountains. ‘The town, however, seems to have been in the
region of transportation rather than of deposition, and the hills of gravel,
moraines, etc., that we meet farther south are lacking. Water-sorted sands
of post-glacial times are present in the stream valleys. The hills are of rock
so far as observed, and the boulders noted were doubtless stranded in the
melting of the ice sheet while they were in transit. All the large boulders

are anorthosites,

600 Report oF THE Strate GEOLOGIST.

Mines There is only one ore-body in the township, so far as I learned,
and that is the Schofield vein on the extreme east, at the line with Ticonderoga.
There are two ore-beds in a ledge, fifty yards or so east of the highway, and
about thirty feet above it. The lower-and larger is about twenty inches
thick, and the upper, a few feet above, is from two to twenty inches.

Naturally this amount is not very serious, but in the earlier days of the

NANG WY Wy

vw Ww,
DL AAYAY AR
WQS

CROW
SKS
SS

SS
aga ES SN

Wer WA ww) Wa owe vi

Ww
. ie Wow we ° SFT.

FIGURE 2.

bloomeries the lower vein was somewhat mined, and excavations thirty or
forty feet down were made. The ore is probably much the same grade as
that at Hammondville, as the wall rock is the same.

In his Bulletin on the Iron Ores of New York, Professor Smock speaks
of another small mine on the north side of Paradox lake, but I learned
no particulars about it.

Ticonderoga.

In my previous report, p. 452, the map of Ticonderoga was left
incomplete as regards its western edge. The observations that were gathered
last season along the western line with Schroon, make it quite evident that
the gneisses of Series I, with perhaps some limestones as yet unlocated and
some minor intrusions of gabbro and trap dikes cover the area. The map has

therefore been filled in on this basis, and appears here in completed form.

Minerva.
Topography. Minerva is a very large township, which is still but
sparsely settled. While its elevations are of moderate character, no specially

notable one being within the town lines, they are, in instances, extremely

rugged and wild. Population is chiefly limited to the southeastern corner, -
£2 p y

‘"TIHSNMOL VOOUAANOOIL AO DVN OIDOTOUD

Ss + © z ' ° OYdaVO YO. 3LISO
SSTIW 40 TIVES SLSIHOS WOV1G GNV
"01a STAVE SS CONWS WVGS.LOd 3NOLSAWIT
PARE z oy mE
TWisv719 : }

WANA
SSIAND:

OWdeYD SLISOHLYONY = JANITIVLSAND

fin

Tr

UD
6.0 NU
6

NY

“ N
Ny XS
~

vas
aS

IIIA ALVTd

fd Cee

YY.

Kremp—Gronoay or Essex County. 601

where Olmsteadville is situated. Scattered houses extend for a few miles
along the highways, but to the north, after three or four miles, there are but a
half dozen until one reaches Newcomb. The same is true of the southwest.
On the northeast the Boreas river flows into and diagonally across the town.
Where it enters, the river is about 1,700 feet above tide and the surrounding
hills are 800 feet and less, higher. Passing southward along the eastern border,
the summits reach 2,000 to 2,500, and as a maximum 2,850 feet. Right at the
corner where the boundary bears away eastward, is Oliver hill, a very large
knob of 2,477 feet. Minerva stream flows southward on the west of it and
Trout brook on the east. A high ridge marks the southeastern boundary. The
valley of Minerva stream is somewhat open and level near Olmstead ville, but
along the southern boundary the hills are again of notable height, and rugged
in the extreme. The valley of the Hudson cuts the northern town line near
its middle point and is narrow, with steep, precipitous hills closing it in. The
town of North River is just over the lime in Warren county, and five miles
still further down is North Creek, the nearest railway terminus. Along the
highway to Blue Mountain lake for several miles after leaving the Hudson,
the ridges are rocky, bare and rugged, but on the extreme west they die away
m open and fairly level country where the lakes appear on the map. Along
the northern border around to the starting point the hills come in again, but
the country is a wilderness, broken only by the camp of the North Woods
Club.

(reology. So far as present observations go, the town is chiefly formed
by gneisses and crystalline limestones, of which the latter are especially
abundant as compared with the other towns studied. On the northeast,
gabbros and related gneissoid rocks appear, and the same are present along”
the eastern border, but the greater part of the town is south of the main
outcrops of the anorthosites.

Series I and JL. It is not feasible to sharply distinguish between these
two at present (even should it ever be so), as observations have not been
accumulated in sufficient amount. The valleys, naturally the places where
the highways are located have, almost without exception, been excavated in
the limestones. The intervening ridges are gneisses. So much of the town
is difficult of access that observations are not yet recorded in great detail.
On the central eastern border the gneisses are met at No. 116b, but south in
the same valley near Irishtown the limestones appear. Along the road at
No. 116c¢ on the west side of the creek, I noted a pile of sulphurous magnetite

said to have been derived from the hills to the westward. It reminded one

602 Report OF THE STATE GEOLOGIST.

of the Lee ore near Port Henry and the Vineyard openings on Buck
mountain, in Ticonderoga. Near Olmsteadville and in the valleys to the
eastward, limestones and the characteristic schists and gneisses that accom-
pany them are frequent. The same statement holds true along the highway
that runs west and then southwest to North River. At No. 110 is a light
quartz gneiss, at No. 111 a white crystalline limestone, and in between are
dark hornblendic schists and thinly laminated gneisses such as usually
accompany the limestone. Quartz veins of inconspicuous character are often
seen. At No. 112, 1n the creek bottom and on the east bank, is a fine out-
crop of a thinly laminated, richly quartzose gneiss. Limestone appears near
the town of North River in the east bank of the Hudson, and further up
stream are cliffs of gneiss nearly 200 feet high. Along the highway to Blue
Mountain lake, alternating exposures of gneiss and limestone are met to the
town line, except just east of No. 115, where a gabbro excessively basic and
somewhat schistose and rich in magnetite appears. From No. 1138, for a mile
or more, a superb fault scarp is on the north side of the road, where the dip
and strike sign is located. It exposes a precipitous front of gneiss, and has
a small prospect hole for garnet well up on its sides.

Passing now along the highway in the eastern central part of the town
from Olmsteadville to Newcomb, the same alternations of gneisses and
limestone exposures are met as far as No. 123, which is a mile or less south
of Aiden Lair. Gneissoid rocks belonging to Series III then appear and
extend off to the northeast beyond Hewitt pond and no doubt connect
with the areas north of Bailey’s pond in Schroon. They are described
under the next series. At the crossing of the Boreas river, quartzose gneisses
‘again crop out at Nos. 125 and 126, but gabbro and black hornblendic
schists lie both south and north of them. Beyond Van de Whacker creek is
No, 128, a coarse quartz-orthoclase gneiss, with the two minerals in lenses
just as was noted for Schroon, No. 97, and Jay, No. 6, the latter from
Haystack mountain.

Along the road that branches off to the North Woods Club near the
middle of the town, black schists and gray gneisses are crossed as far as
the Boreas river. Beyond its bridge, limestone of the usual graphitic white
variety is the principal rock exposed. No. 141 was the last outcrop that I was
able to reach, so that a great area in Minerva and Newcomb to the north-
west remains unstudied, but I have little doubt, both from its abundant
lakes and moderate hills, that it will all prove to contain the usual asso-

ciation of limestones, schists and gneisses.

PLATE !X

y,
Cs

Mee

es
oe
Ae

oS<S
See
SESS PSS
SSO eee ote

XX
aX)
KN
9
a
¢,
a
o

exX)
g
i
xX)
"

ig
‘
’
‘
0,
4
x
?

wy
x)

XXX)
YY
OX)
AX

)
tt
ian

Fixe
FEM)
.

ey, TER
AY WWD
aN i \ oe i

NNN

i CAMBRIAN LOWER SILURIAN GLACIAL
GNEISS ‘CRYSTALLINE ANORTHOSITE GABBRO WER SILURIAN GLACIAL.
J RS BSSsss3 _———— na Feesese sl
SS LIMESTONE POTSDAM SAND === rca’ GRAVELS ETC.
GNEISSOID = aN BLACK SCHISTS SCALE OF MILES
RSSSeSS
ANORTHOSITE OR GABBRO

GEOLOGIC MAP OF MINERVA TOWNSHIP.

Kemp—Grontocy or Essex Country. 603

The strikes and dips that were recorded are plotted on the map, but they
display such variability that no general conclusions can be drawn from them.
They will only be of value in close detailed study in which every outcrop is
noted, so that step by step such structural details may be worked out as are
possible.

Series III. Along the east and west highway in the extreme northeast
corner of the town, gneissoid rocks rich in garnets and doubtless derived from
moderately pyroxenic gabbros and norites, are the rule from Labier’s at the
town line until the line of Newcomb is nearly reached. The usual basic
gabbro then appears and extends across into Newcomb, but near the highway
outcrops do not occur with all desirable abundance. Gabbros or black
gneisses and schists regarded as derived from them are found just south of
Van de Whacker creek at the crossing of the highway from Minerva to New-
comb. I map them as belonging with the gabbros, although from their
general metamorphism, the interpretation is not thoroughly established.
South of the Boreas river, gabbros of the usual basic type do appear, and
to and beyond Aiden Lair and eastward at Hewitt pond, garnetiferous
gneissoid rocks, clearly derived from sheared anorthosites, constitute the
ridges. At No. 123, just north of an abrupt eastward bend in the road, are
typical “ augen” gneisses derived from the labradorite rocks, and with large
nucleal labradorite “ eyes” or “augen,” left in lenticular shape.

In the southwestern part of the town, near No. 115, black hornblendic
rocks are again met which are presumably derived from gabbro. Along the
eastern border, at No. 116b, and to the north the float, even that of a small
size, in the valleys is all of Series III, so that the hills to the north, which
were not easily reached within my limited time, are doubtless of this series
and a westerly extension of the same rocks visited in Schroon, just north of
Bailey pond. They connect the latter with the Hewitt pond exposures
mentioned above.

Series TV was not met, and it is not likely that it was ever present,
unless in the Hudson valley, of which I see no evidence.

Series V. No trap dikes were met.

Series VI. Glacial gravels are not infrequent and boulders of the
massive anorthosites and gabbros from the peaks in Newcomb are very com-
mon along the highways. They furnish very fresh and accessible illustrations
of the general character of these rocks. The large area that is covered by
sand and gravel along the north border, where the highway crosses from

Minerva to Newcomb, begins in Minerva, but is most extensively developed

604 Report oF THE STatTE GEOLOGIST.

in Newcomb. Much sand and gravel also occurs north and south of Minerva
post office, but in the portions of the town that were studied, it must be
admitted that the glacial deposits furnish much less of interest than in the
towns farther south.

Mines. The one little iron-ore prospect referred to under Series I and
II, was the only one | met. The quality of the ore precludes its working.
Professor Smock mentions a vein northwest of Olmsteadville that was opened
by the Burden Iron Co., in 1881, but that is only of small size (Bulletin 7,
New York State Museum, p. 36). The only other mineral of importance is
garnet, but the present developments for it he mostly just outside of the town,
in Warren county. The one prospect that I saw was high up on the precipitous
cliff in the southwestern corner. Although I noted the small dump in the
talus while passing at a distance, I did not learn what it was until after I
had returned to Minerva. No doubt the region is favorable for the mineral,
and some deposits may yet be opened up but, as stated, present developments
are in Warren county. The following brief accounts are all that have yet
been published about them. IF. C. Hooper, “Garnet as an Abrasive,” School
of Mines Quarterly, January, 1895. D. Van Ingen, “New York at the
World’s Columbian Exposition,” p. 341. Further study of them will be of
economic importance as well as of scientific interest in illustrating one of the
minor results of the general metamorphism. ‘The limestones have certainly
been important contributors of their substance toward the formation of the

mineral.

Newcomb.

Topography. Newcomb is a very large and sparsely inhabited township
that lies along the western border of the county. In its northeastern corner
it contains the headwaters of the Hudson in lake Henderson and lake
Sanford, and in Jake Colden from which flows the Opalescent river. Several
high peaks are in this section, for the summit of Mount McIntyre, at 5,112
feet, is just across the line in North Elba, and its southerly ridges at 4,855
feet and less, stretch well into Newcomb. Santanoni, reported at 4,644 feet,
lies some miles westward and is an impressive peak because comparatively
isolated. Coming south along the eastern border, the valley of the south:
branch of the Opalescent river is a fairly open one, and is succeeded by the
North River mountains, a ridge 3,814 feet at its summit. Minor spurs are
characteristic of the southeastern portion, with one good sized lake called

Perch pond, Along the southern line the elevations are moderate, but the -

‘dIHSNMOL GNOOMAN AO TVW OINOTORS
* 5 : $ OWBAVD YO FLISOHLYONV

SaIW 40 a1VvOS ; ESSE
, SLSIHIS WOVIE ONY “GiogsiaN9
“OLE STBAVYD 20" === NWS WVGS.LOd © ,
ieee] TT we Es KEY NNN
TWIOVWTS © NVIBMTIS HSAA0T © NVINEWY9 OYddvd SSIt4ND5.
+ AS Ea = = = - Se = Im at el aS et ig os) eee ee er eee Cee ee ee Ne ene a
Ee TT RID AT] TET PT r
NRRUUuUTuSUnUUUET): Lavell I] | || | Y /
SEER RRR eeE CS ae
SARE EAS a quae ASN Loe Ne: Ny 5
SRRNEERRNSREE CREE OOo o| Mog . /
Seaen SS ae MA oe ba gee
RB : :

6
cH
4

eo
He
HE

Teas
tA MY; \ £600"
SSE ee.

AN SSS SOS GUAT <9¢
TORE =aeu SAY Ni Alin 44,
ay ere tS vA Yas vA \ \
FERRER RAREST AVREREY COU EERE REE a\\ \ hi, Las.
eA SAS TA SHV AL ALATA \ \A > 6
AAS a” as eSes <V RMAC NS \ ¥9 /
TN AAS AI SAAS WH \\) 5
Site oe Wk NE a8 A Sok sl} Vo /
SO GOS UE (RAGE SET Se Ae YAKS J
Pree ee Pe A Ss 4%
A PWERREAR ABA 6.7 ASG eS ! \A\ be
CULL LL LY LN ae Ook “a | eS || vy,
WEE aw NY PN ENS VN oh
A SAE
CYA LAL SEAR wD Ae Dawe
(OORT VAIS OYA
CE ALED AE ARAENE TE al Soe }
ee ae Ce a TOA i
FSS ALAA AAA AAA VAX ICR VAX Aes
RE OSeERE BE BURE ADRS Bre” eee Ey
; AAD AE GA AA oa Uk TA ERA SH), area
2tESERRESGRES -
(TAA TEEN vot
QWERREC Eas ce SOE PU EN ence
A ESS ; wN
Ske QABe BEDE BE! VIED Sony
AS ATABE BS ARE A SKN SEECGER
Ta es Sk
AERESSRERAS AUT
WES SUC eal SeSCOTEnES SAG
was ASRS
“ACES ape
= San

‘ Ney Ah NSN

Se SELES

eV micas wy TEVrer WN
a

SIA eee A ws A

a Naty \
a = eae
XA wee

a
"

Krmp—Groiocy or Essex Counry. 605

country is very wild and but slightly opened up. The Hudson passes out on
the southwest, receiving an important tributary from the Chain lakes. The
western border has the same character of moderate elevations and exhibits the
topography more typical of Hamilton county in which the high peaks disap-
pear except as an occasional one breaks the general stretch of moderate
elevations. Mount Goodnow, Mount Baldwin, Catlin mountain and Moose
mountain, are the chief eminences. Catlin lake, a rather large body of water,
is right on the line. This lake and its tributaries drain south into the Hudson,
but on the northwest and north, the Cold river, rising in Preston ponds, flows
westward into the outlet of Long lake and ultimately into the Raquette river
and the St. Lawrence. The northerly town line passes along the south slopes.
of Mount Seward, and of Wallface mountain, crosses the Indian pass, which
is one of the finest gorges in the mountains, and runs over Mount McIntyre
to the northeastern corner. The central part of the town is a comparatively
open valley with lakes Andrew, Newcomb, Rich and Harris and across a
divide of moderate elevation, lake Sanford, all of which together cover a
good part of its area. The change in topography is largely due to the
presence of crystalline limestones which have furnished an easy mark for
erosion. The highway to Long lake passes along the shores of lake Harris
and Rich lake, and in this portion is the village of Newcomb and the only
settled part of the township, except as regards summer visitors.

Geology. Field work in this town is still very incomplete. I have
crossed the northeast corner at lake Colden, have visited the iron prospects
around lakes Henderson and Sanford, and the outcrops along the Hudson
from lake Sanford to Newcomb. I have gone from Newcomb post. office to
lake Newcomb and coasted around it, and have made another trip to the west
boundary of the town on the Long lake road, and again along the highways to
Minerva and to North Hudson, but the northwestern and the southwestern
portion I have not explored, as they were not accessible in the time at com-
mand. Specimens of anorthosite have been received from the hills around
the Preston ponds, through the kindness of Mr. Charles A. Macy, 2nd.

Series I and 77. It is not feasible with present knowledge to attempt
to differentiate these two, if, indeed, it ever will be. The crystalline limestones
are widespread and have beyond question been a prominent factor im bringing
about the lake basins in the central part of the town and in determining the
river courses. After crossing the Minerva line the outcrops are buried in
gravel until one passes the next cross-roads. At No. 49 is an outcrop of white

crystalline graphitic limestone that was quarried forty or more years ago for

606 Report oF THE STatE GEOLOGIST.

the furnaces upon lake Sanford. On the road to Newcomb the same rock
again appears at several points and furnishes a fine bluff on the south shore of
lake Harris near No. 47.* Black hornblendic gneiss forms a hillock at No. 47,
while just across the bridge leading to lake Newcomb is a green, rather
inassive gneiss, which under the microscope exhibits orthoclase, or at least
untwinned feldspar, some plagioclase, quartz and hornblende. ‘The same rock
is met on the road to Mr. Pruyn’s camp, in some of the borrow pits, and has
been noted elsewhere in the county. Crystalline limestone and its char-
acteristic associated black schistose and quartzose gneisses are met as far
west as the town line. On the road to Newcomb lake, gneisses generally dark
and hornblendic are seen, but on the shores of the lake at No. 131, just north of
Mr. Pruyn’s camp, white limestone again appears, with graphite, brown tour-
maline and blue apatite all in small and poorly developed crystals. This
ledge was also a source of stock for the early furnace near lake Sanford. At
Watch Rock, at No. 132, on the southwest side of the lake, is a quartzose
gneiss, and again at No. 134, called Flat Rock point, there is a dark graphitic
gneiss, Which is doubtless a metamorphosed sediment.

It will be a matter of great interest to determine the geology of the
northwestern portion of the town, because it seems probable from the
character of the country, as seen from afar, that the anorthosites and gabbros
end with Santanoni and that this region of lakes and moderate hills will
prove to be gneisses and limestones. The anorthosites are of course well
known far to the southwest and may form isolated knobs in the region between
Newcomb and the line of the Adirondack and St. Lawrence railroad, and
they are present around the Preston ponds, but the country, so far as scattered
observations indicate, is mostly gneisses and limestones. Much the same is

likely to prove true of the southwestern corner of the town.

Series IIT. The anorthosites and gabbros practically make up the

eastern third of the township. On the highway from North Hudson, gabbro
is met at No. 49b, just east of T ahawus. On the road from Tahawus (often
called the Lower Works) to the old Adirondack village (the Upper Works, or
“Deserted Village”) strongly gneissoid rocks first appear, but near lake San-
ford’s southern end they yield to well-developed anorthosites which form the
hills on each side. At the prospects on the great Sanford vein, at Nos. 43
and 44, the wall-rock is a massive aggregate of labradorite, and little else, and

from the ledges in the river and hillsides, near the present club-house, the

* This is the locality of the fine tourmalines first brought to notice by Professor Beecher and described by Mr. F. L. Nason
in Bulletin New York State Museum, Vol, I., No. 4.

Kremp—Gro.tocy. or Essex Counry. 607

typical coarse, massive, bluish black anorthosite is to be had in endless
amount. It is a beautiful rock and could not fail to impress any geologist as
a most attractive object of study. The dark color of the fresh rock becomes
a pale blue or grey on exposure. Its water-worn pebbles display at times the
characteristic play of colors, and suggested the name Opalescent for the
creek or small river that drains lake Colden. These rocks extend in typical
development to the northeast, and are found in all the peaks around lake
Colden. They form the walls of Indian pass and are present around the
Preston ponds, but how far they extend to the west I can not state from
personal observation.

Lakes Sanford and Henderson are classic ground in connection with the
early metallurgy of iron in this country, and as the result of Professor E.
Emmons’ Report on the Geology of the Fourth District, in 1841, the
knowledge of the enormous deposits was spread abroad and no doubt in part
through the influence of this report the historic old furnace was con-
structed. More extended mention of it is made later on, but the purely
scientific question of the relations of the ores to the wall-rock may be
here discussed. The question is a quite different one from that of
the ordinary lenticular deposits of magnetite, parallel to the laminations
of gneisses. The ores are titaniferous in varying amounts up to a max-
imum “of nineteen per cent. The walls are a perfectly massive plutonic
rock, consisting of little else than labradorite. At the mill-dam opening,
where the wall-rocks are the best exposed of any, and on each side of
twelve to fifteen feet of pure ore, they are of exactly this type and
are perfectly unmetamorphosed. In the river bed near the iron dam or
ledge of ore that makes a little reef, and at the mouth of Calamity
brook, the ore is mixed through the rock in clots of all sizes, from that of a
nut, upward. In the ore itself are found large plagioclase crystals of dark
green color because so charged with dusty augites as to be opaque, even in
thin section, and around the edge of each feldspar and separating it from
contact with the ore is a rim of brown hornblende and biotite, up to an eighth
of an inch (three millimeters) thick. ‘These plagioclase crystals are almost as
large as a man’s hand as a maximum, but they are usually one or two square
inches in area. They are not strained, so far as my observation goes, and they
show the twinning striae sometimes even to the unaided eye. The best place
to study them is at the Sanford bed in the prospect opened up on the hillside
about a mile from the lake, approximately at No. 44. There seems no escape

from considering these ores as of true igneous origin, separated from a cooling

608 Report oF THE STATE GEOLOGIST.

and crystallizing magma, and concentrated by those magmatic changes,
regarding which we are accumulating many observations, but of whose causes
we yet know little. This same view has been advanced in my previous
reports for the smaller ores in gabbros and, as all familiar with the literature
know, it is the explanation advanced in later years for the parallel occurrences
of titaniferous ores in Scarfdinavia. It merely assumes an abnormal richness
in favored lecalities of one of the normal but subordinate minerals of these
rocks. Details of the size, composition and location of the ore-bodies are
given in a subsequent paragraph.

Series IV. There are no Palaeozoic sediments in the township.

Series V. No diabase or other dikes have been met, but there is little
doubt that such exist.

Series VI. There is a great deal of drift and gravel south of Tahawus
post office, and from there to and beyond Newcomb post office. The borrow
pits of the fine highway from Newcomb to Mr. Pruyn’s camp on Newcomb
lake, give excellent: sections and exhibit large boulders often mingled with the
finer gravels. The boulders are all of anorthosites or related rocks that have
been brought down in great quantity from the mountains on the north, and
that supply the most convenient means of studying their varieties.

Iron Mines. The only iron mines of the town are those around lakes
Sanford and Henderson, which were opened about 1840. Rumors of the
existence of the ore reached the settlements some five years or more earlier, so
that an expedition was organized in 1886 and another in 1837, that went in to
lake Henderson and brought back reports about the district.* The Natural
History Survey of New York was organized at about this time and in the
next few years the annual reports of Professor Ebenezer Emmons, who had
charge of the work in this part of the State, make extended mention of the
ores. Professor Emmons was profoundly impressed with their abundance and
extent and regarded them as among the most important resources of the state.
In his final report+ he gives a fairly complete description and urges their
development. Soon after this a small blast furnace was erected, of five tons
daily capacity, and some years later a larger one of twelve to fifteen tons,
together with puddling furnaces and the necessary machinery for making bar
iron.{ The latter stack is still standing and the accompanying illustration is
from a photograph taken by the writer in September, 1894. Mr. Rossi gives

* W.C. Redfield, Some Account of Two Visits to the Mountains of Essex County, N. Y., 1836-1837. American Journal of
Science, i. XXXIII., 301.
+ Report on the Second District, p. 244, 1842.

t See A. J. Rossi—Titaniferous Ores in the Blast-Furnace ; Transactions American Institute of Mining Engineers, XXI.,

pp 832, 1893. Especially p. 835.

PLATE XI

WYNKOOP HALLENBECK CRAWFORDCO.

VIEW OF THE BLAST FURNACE AT THE ‘'UPPER WORKS" ON LAKE SANFORD THIS FURNACE
WAS BUILT ABOUT 1852; ITS LINES ARE GIVEN BY A. J, Rossi (TRANS, AMER. INST.
MIN. ENG, XXI, PAGE 837). PHOTOGRAPHED BY J. F. KEMP, 1894.
SEE PAGE 608.

A)’

“ae

Kemp—Gerotocy oF Essex County. ; 609

the working drawings of the furnace in his paper just cited. The furnace
went out of blast about 1859, and the enterprise stopped after having been in
operation fifteen or eighteen years, during which the manufactured
iron made its labored exit to the markets by means of teams to Crown Point,
some fifty miles distant. The expense of haulage proved too serious. The
early promoters-of the enterprise have found enduring memorials in the local
geographic names, Henderson, Colden, McIntyre, ete. Emmons seems not
to have known that the ores were titaniferous, nor so far as can be learned
were the later operators, at least for some years, aware of this fact. In view
of the great prejudice against titaniferous ores to-day this seems remarkable,
because, so far as we know, these comparatively primitive furnace men found
no difficulty in smelting the ores. The question of their peculiar properties
and behavior in the furnace has been taken up in extensive experiments in the

last two or three years by Mr. A. J. Rossi* with very encouraging results.

With multi-basic slags and high percentages of TiO, in them—say twenty
to thirty-five—no trouble was met in a low small stack from their reputed
infusible properties. The question is an interesting and important one, and it
is much to be hoped that it may be solved in the large way and that these
great reserves of titamiferous ore may be made available.

The ore-bodies at present exposed are in the situations shown by the
accompanying map. The map has been traced in outline from one that was
made for the iron company about 1850 and that was engraved and printed.
One of the few copies known to be extant was kindly loaned to me by Mr.
James MacNaughton for this purpose. In transcribing, some topographic
shading has been omitted, and one or two additional names, signs for mines,
etc., have been introduced. With one or two corrections, the map is
practically the same as that made and printed by Professor Emmons in his
early report. The map of 1850, from which the present one here introduced
was traced, is smaller than Emmons’s original. The long side of the latter is
approximately twenty-one inches, while the long side of the former is fourteen
inches. ‘The present map is nine inches on this same line,

An old opening is northwest of lake Henderson, but I have not seen it.
A short distance below the Upper Dam, at the outlet of lake Henderson, is
the Millpond opening, on a mass twelve to fifteen feet wide, striking nearly
north and south and dipping about 75° KE. Its location is shown approxi-
mately by the crossed hammers. This was one of the chief sources of ore for

the early furnace, so that a pit now remains about twenty-five feet or more

* A.J. Rossi, Op. cit.; also, The Smelting of Titaniferous Ores ; ‘‘ The Iron Age,” Feb. 6 and 20, 1896.

39

610 Report oF THe Strate GEOLOGIST.

on the strike and of depth not visible, as it is full of water. The wall rock is
massive dark anorthosite, practically pure labradorite A line of strong
attraction runs north and south along the east side of the Adirondack river.
There is a little show of ore where it crosses Calamity brook, but the amount
visible is not great. I was informed by Mr. Buttles, who was in charge of the
“club house, that it had been opened at the north, where the word 7ron-ore
appears on the map. The “Iron Dam,” so widely known in connection
with the region, crosses the river just above the present club house, and
shows as a black strip, striking approximately N. 25° E. The ore is more or
less mixed with anorthosite and appears to be an integral part of the rock.
In the rear of the ice houses that stand to the west and a short distance back
of the club house, there are openings on another body of ore which is revealed
ina small excavation. A breast several feet across is exposed. The strike is
somewhat indefinite, but the ore bears westerly into the hill.

This entire belt of ore along the river may perhaps be considered as a
single one of many individual masses. The ore afforded was called “ Black
Ore,” and the name is still perpetuated on the map given above. Professor
Emmons regarded the belt as essentially a single one with many individual
masses separated by intervening walls of rock. He also states that
“hypersthene, labradorite and small masses of serpentine” were the only
foreign admixtures. It is of mineralogic interest that he cites one or two
inclusions of pyrites, the size of a butternut, for sulphides are very rare in
titaniferous ores. Professor Emmons gives the extreme width of the belt as
over 700 feet, and its length as 3,168 feet. Its general character of large
masses in the midst of wall rock which is also massive, lends itself to an
interpretation of igneous origin with greater readiness than to any other.
Great quantities of ore were obtained from the float for the early furnace.

Ore from the Millpond opening was largely used by Mr. Rossi in his
experimental run, and several analyses have been published by him to which
are added two that I have received directly from him. The analyses show
that the percentage in titanic acid is quite variable, ranging in round numbers
from ten to twenty. The percentages in iron hold at very good values, and
the phosphorus and sulphur are extremely low. The alumina and silica are
in small amount in the first two and suggest the presence of labradorite, but
the high alumina of the third is difficult to explain on any other supposition
than that some form of spinel is in the ore. Titaniferous ores high in alumina
have been met in Westport township, and the same inference is still more

strongly suggested by them.

sandr

Tron Ore

PB

.

s

/ =

i Sanat OLS Bed

A
“Ororo

a

Chure k
Tubol Cai

7° —
Fine Gramed Oje

GROUND PLAN
of Beds and veins of
MAGNETIC OXIDE OF TRON
Traversing theHypersthene ana Feldspath ic Rocks at

ADIRONDACK,
Essex County, NewYork
Oa Pest of tract owned by the MacIntyre lron Co
Mop drawn from Survey notes made

at the time of Prof. Emmons’ report,
Lt) 4 ih. the =o

‘sx-Fvon Ove ~~
ee

e
‘)
oO
\&
er
i
ae
\ X

_ ae

Kemp—Gronocy or Essex Counry. 611

Pert |. Rosey: Rosst. Rossi. | Lepovx.
Pa eo | 3.67. -|. 1.53. - 0.91
tt eee eee eT LOLS | L388 19.74 20.24 | 20.49
KO eee et el 0.44 \. 1.50. | 3.50
(CONOR S929 SA ae a or little | little
Rinameeeee a SR Pac cuh le trs 1 | -0L50.- | 2,60
Omer: cures t AO OTS
Oe ee re | 87120" | 89.87 °| 73.62
MES Noe” aR el is ck tes none |» 0. O17). 0.037
Sa 8 Se Seine © 1a none | 0.068 | 0.08
Om fete le ce | Goa 4ou |! "59. 56 53.62 55.62 | 54.80

After engaging a guide and a boat, I rowed down the river and coasted
the east shore of lake Sanford to a point somewhat east or south of east from
Big island. We then walked about three-fourths of a mile up hill to the east,
to an opening on the Sanford ore-bed, very near the location of the crossed
hammers on the map. Considerable ore had been blasted and taken away a
short time before. The location was about 300 feet above the lake. A breast
about thirty feet wide by fifteen feet high was exposed with no wall rock
appearing. It apparently trended northeast, as I followed float ore with no
outcrops for a hundred yards. All the loose surface rock met was anor-
thosite. The ore both in the lump and in the breast ‘contains occasional
crystals of green plagioclase, in instances three or four inches in diameter.
They show the characteristic situations, but are so thickly charged with
minute green augites that a millimeter from the edge, as shown by thin
section, they are practically opaque. Each is surrounded by a reaction rim, two
to three millimeteys wide, of biotite and brown hornblende, so that in no case
does the feldspar actually touch the ore. They are extremely curious and
interesting phenomena. Undoubtedly the feldspars are original crystalliza-
tions from the igneous magma precisely like the ore itself, and becoming
involved in it, these rims of minerals of intermediate composition were
produced by the reaction of the two on each other. Some samples of ore
have given curiously high percentages of alumina, and, as earlier remarked,
these included feldspars are in part responsible for it.

612 Report oF THE STATE GEOLOGIST.

The open cut gives no indication of the actual size of the ore-body except
so far as the failure to reach the walls imphes that it is large. A line of
attraction has been traced down to the lake, however, across it and on the
other side where the name Sanford appears again. A second line of attraction
has also been noted crossing the lake further south.

In Professor Emmons’s day, four sections were uncovered on the east side
of the lake, across this vein by trenching. The longest were 564 feet and 610
feet respectively, and they exposed ore with occasional streaks of rock for the
entire distance. These trenches have long since become filled in, but there is
no doubt that the supply of ore is enormous. By the -heavy lines running
into the Sanford ore-bed I have endeavored to locate these trenches as
accurately as possible from the descriptions of Professor Emmons. Were
mining again begun, the Sanford ore would naturally be the one first attacked
and the indications are favorable to many years of open cut work above the
level of the lake.

The composition of the ore is shown by the following analyses of which
the first four are given by Mr. Rossi in the Zron Age, February 6, 1896 :

pares Jee See
| HO rid" 3
SiO... -. os | O58) 22246" wigs lege abe Os
TiO, .-. ...|)10,91 |, 20,08 | 19-52 91/18: 700) 1459) eel eaead
ALO, «2 2. \ 0558 4 oenOamaen 5.81 |
CaO . |
MpOuu. > | |
MnO, 8 | | |
Re,O,. 2 | 87260" EyOsye4|- wo ce Oe om|
1g ye enone 0.022
S i. eo. ee) One 0.028
Fe ... . .| 62.65 | 51.22 | 51.80 | 51.44 | 56.60 | 62.66 | 36.86

Experimental attempts to concentrate the ore with magnetic machines
were made some years ago in the hope that the richly titaniferous portions
could be separated from the non-titaniferous, on the assumption that the

latter variety was more highly magnetic than the former. All such experi- —

Kremp—Groitocy or Essex County. 613

ments are of course based on the supposition that titaniferous ores are
mechanical mixtures of normal magnetite with ilmenite, but there is little
reason to doubt that where the percentage of TiO, is considerable, say ten
and above, the mixture is either so intimate as not to be economically broken
up, or else it is actually a chemical combination in the nature of ilmenite or
some related mineral. Mere magnetism does not preclude titanium, for O. A.
Derby has found in Brazil, natural lode-stone with twenty per cent. Ti0,.

Indications of ore have been met across the divide to the east of the
Sanford ore-bed and in the watershed of the Opalescent river. I have not
visited the locality, as but little work has been expended on it and none in
fact since the early operations. :

About a mile west of lake Sanford is the Cheney ore-bed that presents
some differences both in composition and in wall rock from others. Professor
Emmons, on Plate III of his report, calls the wall rock “sienitic,” but it
really is a gneissoid variety of gabbro, having a laminated structure visibly
developed, while the minerals are those of the familiar gabbros of the
region. Dark silicates are much more abundant than in the anorthosites that
form the walls of the other veins. I did not personally visit the Cheney
exposure, but specimens of the ore and wall rock were obtained by Mr. James
MacNaughton and kindly furnished to me. I understand that forty or fifty
feet of ore are exposed without showing the walls. The following analyses
illustrate the composition. They were published by Mr. Rossi in the
Iron Age, February 6, 1896.

WILBUR. Rosst.

(RicH ORE.) (Poor ORE.)
SiO, Se fe)
TiO, 8.25 LEE
BLOne Told
CaO 8.89
MgO 3.00
Mn,0O,
Fe,O, BPS Fe achiaidh - sai) 86.53 55.64
S “re ate 74 1.00
Fe TENE Ble te ee Ack eM, Oe sce os 62.15 40.338

614 Report oF THE STATE GEOLOGIST.

The ore runs higher in phosphorus and sulphur than any of the others
yet analyzed. Mr. Rossi has also noted in his experiments, indications of the
presence of vanadium, which has been recognized both in Scandinavia and in
New Jersey as one of the characteristic ingredients of titaniferous ores. The
high alumina in the second analysis, much above any aluminous silicate that
might be present, is worthy of note, and the same is true of the lime. Some at
least of the magnesia is combined with iron oxide and silica to yield hyper-
sthene ; some perhaps with lime and alumina for augite. Some of the lime
may be united with silica and titanic oxide to give titanite and some with
alumina and silica to form labradorite ; but in whatever way the combinations
are worked out, there remains an excess of alumina and lime, so that the
probability of spinel being present is heightened.

Professor Emmons mentions other ore-bodies whose presence was demon-
strated in his time, viz., a vein of “fine-grained ” ore about eighty rods east of
the works. It would be on the map at or near the southern prolongation of
the “ Black Ore” belt, but as he states (page 254) that it was 150 feet across
and 5,742 feet long, it must be distinct from this vein as mapped. He also
cites much float-ore along East river (now called Calamity brook). Since his
time float-ore has also been located to the northwest toward the Preston
ponds. The magnetic surveys of Mr. Sebenius have indicated strong attrac-
tion under the lake and on its shores south of the Sanford belt, and still
additional localities of attraction have been met near the Lower Works (now
called Tahawus post office) in the gneissoid rocks of that section. In fact,
the more one collates the accumulated data, the more one shares in Professor
Emmons’s impression of the large amount of ore that is present.

For the ore-bodies in the massive anorthosites, the only conception that
fits their mineralogic character and geologic associations is that they are
great bodies of titaniferous iron oxides, segregated from a vast plutonic magma,
through whose crystallized substance they are now distributed in broad and
somewhat roughly outlined belts. All gradations can be found from pure
metallic oxides to pure masses of labradorite.

As regards their future development, if brought about, it will be by
means of an extension of the Adirondack railroad up the valley of the
Hudson, along the route that can be easily traced on the maps of Minerva
and Newcomb. The grades are gentle and the engineering difficulties are

slight.

GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

SECTIONS AND THICKNESS OF THE LOWER SILURIAN
FORMATIONS ON WEST CANADA CREEK AND
IN THE MOHAWK VALLEY. |

COMMUNICATED BY

CHARLES S. PROSSER anp EDGAR R. CUMINGS.

James Harn, State Geologist.

Sir :—The accompanying paper gives a detailed account of the rock
sections at various localities in the West Canada creek and Mohawk river
valleys. The results obtained serve to show that the Calciferous sandrock
and Utica slate have a much greater thickness than that noted in previous
descriptions of these formations.

Respectfully yours,
CHARLES. S. PROSSER,
EDGAR R. CUMINGS.
Union Cottrecr, Scnenrctrapy, N. Y.

617

‘ALIHM\ SO '5Q ANOZ

“99 GHO4MV4o MOJENAT WHO

3H |

‘AONVLSIG

ANVd
43H! NI

LSSM AHL NO NMOHS 115M
Viv4 NVWYSHS HLIM ‘ONA YaMOT WOYS

| 31V1d

. SMOYYVN 5

AHL 4O MAIA

SJ)

uJ

Sections and Thickness of the Lower Silurian Formations on
West Canada Creek and in the Mohawk Valley.

By CuHarwes S. Prossrr ann Epear R. Cumries.

ContTEnTs: Introduction, p. 619. Trenton Falls, p. 620; Section of Trenton Falls gorge, p. 620.
The Newport Sections, p. 627; Section of the Newport railroad cut, p. 627; Section of the Moshier
quarry, p. 631. Little Falls, p. 632; Section northeast of Little Falls, p. 633; Section of the Cook
quarry, p. 686. Canajoharie and Palatine Bridge, p. 687; Shaper quarry, p. 637; Canajoharie creek
section, p. 688; The Mohawk Valley Stone Co. quarry, p. 640. Sprakers, p. 641; Flat creek section,
p- 641; West Shore railroad-cut section, p. 642; Section at Yosts, p. 648. Tribes Hill and Fort
Hunter, p. 644; North side of the Mohawk, p. 644; South side of the Mohawk, p. 646. The Amster-
dam-Hoffman Region, p. 647; Section along Morphy creek to the top of Adebahr hill, p. 647;
Minaville section, p. 649; The Eva’s kill section, p. 652; Section opposite Crane’s Village on the
south side of the Mohawk river, p. 653; Hoffman and Van Epps hill section, p. 655; Patterson-
ville section, p. 656.

INTRODUCTION.

A recent paper describing the geology of the vicinity of Trenton Falls
contains this statement: ‘The writer was unable to find a detailed tabula-
tion of the stratigraphy or local geological boundaries of the type section
[of the Trenton formation |.” *

In that paper its author has given a detailed account of the strati-
graphy and faunas of the various zones along the gorge of West Canada
creek, at Trenton Falls, based upon extensive collections of fossils from the
entire length of the gorge; these were carefully identified and assigned to the
various zones into which he divided the section. In a recent examination of
the gorge, made by the writers, some differences in the stratigraphic details
were noted, and in order that the description of this interesting formation at
its typical locality may be as accurate as possible, it is considered advisable
to publish the following section and, in addition, to give some account of the
formations in the vicinity of Newport on West Canada creek, which were

also described by Mr. White.

* The Faunas of the Upper Ordovician strata at Trenton Falls, Oneida Connty, New York ; by Theodore G. White. Trans.
actions New York Academy of Sciences, Vol. XV, April, 1896, p. 71.
619

620 Report oF THE STATE GEOLOGIST.

Trenton FAtts.

The rock section begins near the southern end of the path on the western
side of the gorge and extends to the top of Prospect quarry, a distance of
about two miles. The path may be followed for a short distance below the
hotel stairs; but the lowest rocks, stratigraphically, are exposed in the
Narrows above this point. At the water level below the hotel stairs, is the
base of Mr. White’s section D of station No. 130, which also extended from
this locality up the gorge to the Prospect quarries. Section C, No. 130, on
the eastern side of the gorge below Section D, was studied by Mr. White,
but apparently no considerable thickness of lower rocks was found.

Section of Trenton Falls Gorge.*

A’. The lowest rocks exposed along the path on the western side ,f°*,,
of the gorge, are twenty-four feet thick at the Narrows, and on account
of the heavy dip down stream, show only the upper eleven feet at the
southern end of the path. The upper part is composed of thin layers, three
to five inches thick, which form a somewhat clearly defined band two and one-
half feet thick. This is Nos. 3 and 2 of White’s section. Below this band
are similar limestones with shaly fossiliferous partings. In the Narrows, the
lowest layers are compact bluish grey, thin-bedded limestones, interstratified
with coarser-grained layers containing numerous well-preserved specimens of
Monticulipora (Prasopora) lycoperdon. The more compact layers are
unfossiliferous. In the Narrows are shown Nos. 3, 2 and 1 of White, and
apparently about thirteen feet of lower rocks.

1. Monticulipora (Prasopora) lycoperdon, (Say). (aa)t
2. Orthis (Dalmanella) testudinaria, Dal. (7)
3. Plectambonites sericea, (Sowb.), Hall and Clarke. — (r)
4. Ceraurus pleurecanthemus, Green. (7)

Crinoid segments.

Or

A*, Heavy bed of compact, regular, thin-bedded, very dark blue ,f°%',,
limestone, from eight to ten feet thick, which separates into layers from three
to ten inches in thickness, divided by. shaly partings. This heavy bed is
prominently shown along both sides of the gorge from the southern end of
the path on the western side, to the upper part of Sherman fall. At the end

of the path, where the rods are placed, the base of this bed is about eleven

* Station No. 48, Section A. Union College Survey.
+ The relative abundance of the species is indicated in the following manner: a = abundant; aa = very abundant ; ¢ = com-
mon ; Tf =rare ; rr= very rare, when but one or two specimens have been found.

621

E.R.Cumings.

SECTION FROM
FOOT OF TRENTON FALLS GORGE
TO PROSPECT QUARRY

PRossER AND Cumines—Lowerr Sivurtan SECTIONS:
No.48,

- % " a ri rs .

~ DK ~N > ~ e b
Bilas qe ce eae ES 5
8g aR SS Pi K
ey Sor 4 = $

: 3 H cee tA ‘ & nea *
sx as U a ; & i Ca : a e 2 ! a! i !
= Gai CAAA HH A gue THA it Tn n Ae CHR manana: ngage TT i] , ~

ee a ou ae i ae Te iit i ae te eH He HN ia a i it a St ne : ne | tt ae
asa tie i oe Ht ita i en a ea Ue AH ia He =
iTS (HH] Y <! |
Ee oe :

6

slay

meh

ih ne 18 TTT

mayne maapecgial i ai iran Tr i at i ve RAH
ii nt tt cet ct a He fits HH iil nu mh ae a
Te i cee a aly A Hn Ht a it stig tt He i a
8 8 8 wees

622 Report oF THE STATE GEOLOGIST.

feet above the creek level. A little above, is the foot of the hotel stairs on
the heavy bed two and one-half feet above its base. Opposite the hotel
stairs, this bed is not as sharply shown as in the gorge above, on account of
the presence of soil and debris, but it has a thickness of at least eight feet.
Rather more than half way from the hotel stairs to Sherman fall, the gorge
becomes very narrow and may appropriately be called the Narrows. This
part of the glen is well shown in Darton’s picture of the “ Lower Gorge at
Trenton Falls.”"* At the Narrows the dip is 3° 8., but it is variable in this
part of the glen. At this point the base of A? is twenty-four feet above the
creek level, giving the greatest thickness of the lower rocks found in this
part of the gorge. This heavy stratum is readily followed along the side of
the gorge from the hotel stairs to the Narrows, and may be traced by the eye
along the eastern bank nearly all of the distance to the place where it forms
the conspicuous bed in the upper part of Sherman fall. Its base is the
second noticeable line below the top of the eastern part of Sherman fall.
This bed was also traced along the western bank from the Narrows to Sher-
man fall, where it meets the same bed of the eastern side in the mural front
of the fall. At the Narrows and in the cliff opposite Sherman fall it has a
thickness of ten feet. This zone is No. 4 of Mr. White’s section, which he
described as it occurs at the hotel stairs, but he failed to trace it up the gorge
to Sherman fall. White’s No. 7, described as “the broad seam seen in
Sherman fall,” is the same as his No. 4; and Nos. 5 and 6, given as between
Nos. 4 and 7, belong below No. 4.

A®, From the top of the heavy bed to the base of the dark blue ,7%4,
massive stratum above Sherman fall. The rocks consist of thin layers of
limestone with shaly partings and are well shown in the cliff along the path
opposite the top of Sherman fall. In the upper part, corresponding to D”

of White, are abundant fossils, as may be seen from the list below.

1. Monticulipora (Prasopora) lycoperdon (Say). (1)
2. Diplograptus amplexicaulis, Hall. (7)
3. Trematis terminalis (Emmons), Hall. (7)
4. Rafinesquina alternata (Con.), H. and C. (7)
5. Strophomena ct. Scofieldi, Winch. and Schuch.t ()
6. Orthis (Platystrophia) biforata (Schl.), Bill. (r)
7. Orthis (Dalmanella) testudinaria, Dal. (c)
8. Plectambonites sericea (Sowb.), H. and C. (aa)

*Thirteenth Annual Report of the State Geologist |New York], 1894, p. 11. See also Plates I and II of the present paper.
+ Kindly determined by Professor J. M. Clarke.

'

‘ALIHM JO

110 GONV +Q SSNOZ ONIMOHS ,,'SMOYNNVYN,, SHL LY WNVG 1SSM 3O MSIA YSYVAN

110
Il 3LWId

Prosser AND Cuminacs—LoweEr SrmurtiaANn SECTIONS. 623

9. Zygospira recurvirostra, Hall. (c)
10. Bellerophon bilobatus (Sowerby). (r)
11. Asaphus platycephalus, Stokes. (c)
12. Calymene callicephala, Green. = C. senaria, Con. (c)
13. Ceraurus pleurexanthemus, Green (?). (r)

This zone includes Nos. 8, 9 and 10, of White, the combined thickness of
which is twelve feet, the same as that in the present section. (Plate IIT.)

A‘. A stratum of massive dark blue limestone conspicuous in ,*%
the side of the gorge along the path above Sherman fall, varying in thickness
from two feet, seven inches, to two feet, ten inches, called for convenience
in the general section, three feet. On weathering, the stratum splits into thin
irregular layers similar to those immediately above and below. This promi-
nent stratum is a convenient stratigraphic mark for this part of the section
and is clearly shown in Figure A Plate IV, of White’s article, where it is
described as D" of his section.

A®, The heavy blue stratum may be readily followed to the foot ,,¥et,,
of the lower fall of High fall, and A® includes the rocks from the top of
this layer to the base of a conspicuously contorted stratum opposite the top
of the lower fall of High fall. The rocks are thin and shaly in the upper
part with thicker layers in the lower part.

A®, From the base of the contorted stratum to the crest of the ;,"°.,
upper part of High fall. The folded stratum is well shown in Figure A,
Plate Il, of Mr. White’s article. The rocks are thin-bedded. Both the
lower and upper portions of High fall, or zones A® and A® of this
section, are shown in the accompanying plate (IV). The following species

were collected in A®:

1. Monticulipora (Prasopora) lycoperdon (Say). (c)
2. Stictopora, sp.

3. Rafinesquina deltoidea (Con.), H. and C, (aa)
4. Orthis (Platystrophia) biforata (Schi.), Bill. (rv)
5. Orthis (Dalmanella) testudinaria, Dal. (aa)
6. Plectambonites sericea (Sowb.), H. and C. (aa)
7. Tellinomya dubia, Hall. (7)
8. Endoceras proteiforme, Hall. (c)
9. Cyrtoceras, sp. (1)
10. Asaphus platycephalus, Stokes. (aa)

11. Crinoid segments.

624 Report oF THE STATE GEOLOGIST.

A‘. From the crest of the upper part of High fall to a stratum ,,fe*t,.
at the top of the small fall below the Adirondack railroad bridge the rocks
have a thickness of ten feet and two inches. A somewhat conspicuous
stratum, near the crest of the upper part of High fall, may be followed
along the bank as far as the bottom of the small fall below the railroad
bridge. The rocks are thin-bedded, rather coarse-grained and fossiliferous.
Zones A®, A® and A‘ of the present paper, with a total thickness of 138 feet,
are approximately equivalent to zones D®, D®, D, D® and D", of White, with
a total thickness of 166 feet. The greater part of this difference is in
the thickness of the rocks forming the lower part of High fall, which
measure by the Locke level seventy-seven feet, while they were estimated as
107 feet in thickness by Mr. White.

1. Orthis (Platystrophia) biforata (Schl.), Bill. (a)
2. Orthis (Dalmanella) testudinaria, Dal. (c)
8. Rafinesquina alternata (Con.), H. and C. (7)

4. Crinoid seginents.

A®. This zone extends from the stratum noted at the top of the ,7@%,,
falls, just below the Adirondack railroad bridge, to the base of the massive
crystalline limestone which forms the upper part of the cliffs above the
railroad bridge. At this bridge is an excellent locality for measuring its
thickness, the base beg marked by the rather heavy stratum which may be
traced from the top of the small fall below the railroad bridge to the vicinity
of the railroad pier; and its top by the base of the massive limestone out-
cropping near the top of the cliff under the railroad bridge. This zone,
capped by the massive limestone, forms the sides of the gorge from below
the railroad bridge to Prospect village. It corresponds with zones D%, D®,
D*, D* and D®, of White, which were given as approximately eighty-seven
feet in thickness. They are thin-bedded, compact limestones, part of the
strata somewhat crystalline, separated by shaly layers. This zone contains
numerous fossils, some layers having large numbers of Orthis (Dalmanella)
testudinaria. At Prospect, along the sides of the creek from a little distance
below the falls to the highway bridge, is a good place for collecting. The
surfaces of some of the highly inclined layers, by the side of the creek just
above the highway bridge, show a large number of fragments of Asaphus
platycephalus. At the upper end of the gorge the rocks are very much
tilted, exhibiting the greatest amount of folding seen im any part of the gorge.
The cliff on the eastern side of West Canada creek above the Adirondack

railroad bridge is well shown in Plate V. The massive crystalline

LSv4

'YSLVM SHL SAO8Y 1SNf 3GIS 1SAM SHL NO ;,Q SNOZ GNY
JO 30IS 1SV3 SHL NO NMOHS ‘SLIHM\ 40 ',GQ=+G 7

L = We “

39037 3uva 3SHL

=

SMOYYVN », SHL SAOS¥Y WOYS W1V4 NVYNYSHS

1SSM

ProssER AND Cuminas—LoweEr SILURIAN SECTIONS. ~ 625

limestone of A* forms the upper part of the cliff, while the thinner lime-
stones of A® form the middle and lower part of the cliff. The following

species were collected in A‘.

1. Monticulipora (Prasopora) Lycoperdon (Say). (c)
2. Lscharopora recta, Hall. (1")
3. Trematis terminalis (Emmons), Hall. (1")
4. Rafinesquina alternata (Con.), H. and C. (c)
5. Rafinesquinae alternata var. nasuta, Con. (1)
6. LRafinesquina deltoidea (Con.), H. and C. (1)
7. Strophomena cf. Scofield’, Winch, and Schuch. (1)
8. Orthis (Platystrophia) biforata (Schl.), Bill. (c)
9. Orthis (Dalmanella) testudinaria, Dal. (aa)
10. Plectambonites sericea (Sowb.), Hall. (a)
11 Zygospira recurvirostra, Hall. (7)
12. Asaphus platycephalus, Stokes. (c)
13. Calymene callicephala, Green. (c)
14. Ceraurus pleurecanthemus, Green. (1)
15. Leperditia fabulites, Con. (1)
16. Hndoceras proteiforme, Hall. (1")
17. Orthoceras, sp. (1)
18. Lellerophon bilobatus (Sowerby). (1)
19. Dendrocrinus gracilis (Hall). (aa)

20. Crinoid segments.

A®, Massive grey Trenton limestone of the Prospect quarries, a"°%o
twenty-six feet thick in quarry on north side of creek near Prospect, burned
for quicklime and also used as a construction stone. It forms the top of the
steep cliffs along the upper gorge from the Adirondack railroad bridge to a
point above the highway bridge at Prospect. This massive crystalline lime-
stone in moderately thick layers, contains numerous fragments of fossils,
though the number of perfect specimens is small; while in the thin, black,
shaly layers fossils are common. This zone corresponds to D”, of White,
which is given as twenty feet thick. Conrad, in 1837, stated: “ North of
Trenton Falls there is a capping of grey crinoidal limestone,”* and he

undoubtedly referred to this division of the Trenton limestone.

1. Monticulipora (Prasopora) lycoperdon (Say ). (a)
2. Stictopora cf. acuta, Hall. (1)
3. Dendrocrinus gracilis (Hall). (c)

* First Annual Report Geological Survey, Third District, New York (Assembly Document No. 161), p. 164.

+0

626 Report or THE State GEOLOGIST.

4. Rafinesquina alternata (Con.), H. and C. (c)
5. Rafinesquina deltoidea (Con.), H. and ©. (c)
6. Orthis (Platystrophia) biforata (Schl.), Bill. (a)

7. Orthis (Dalmanella) testudinaria, Dal. (a)
8. Plectambonites sericea (Sowerby), H. and C. (c)
9. Zygospira recurvirostra, Hall. (r)
10. Asaphus platycephalus, Stokes. (c)
11. Calymene callicephala, Green. (c)
12. Ceraurus pleurexanthemus, Green. (r)
13. Murchisonia gracilis, Hall. (r)

14. Orthoceras.

The total thickness of this section from the lowest exposures in the
Narrows to the top of the Prospect quarries, as determined by the authors
- with tape and Locke level measurement of the various parts, is 270 feet.* This
amount, however, does not give the thickness of the formation, since neither
its top nor bottom is shown at Trenton Falls. The thickness of the same
section, as given by Mr. White, is 325 feet,+ while Mr. Darton stated: “The
greatest development of the Trenton which I have observed is at Trenton
Falls, where there appears to be a thickness of 120 feet.”{ In 1838, Vanuxem
said “at Trenton Falls, the thickness is upwards of one hundred feet,” $

though in his final report he simply states that the sides of the gorge are

* Recently the writer partly remeasured the section using an Abney’s level and obtained the same result, 187 feet, for the thick-
ness of the rocks from the creek level in the Narrows to the top of Mill Dam fall. The thickness of the rocks from the foot of
High fall to the top of its lower part, is’ sixty-seven and one-half feet; to the contorted layer, eleven and one-half feet more ; from
the base of the upper part of High fall to its crest, forty-eight feet ; and from that stratum to the top of Mill Dam fall, twenty-
two feet. From the foot of the railroad pier, which rests on the top layer of Mill Dam fall, to the base of the massive crystalline
limestone, I obtained sixty-two feet, making the total thickness of the section 275 feet. c.s P.

+ Transactions New York Academy of Science Vol. XV, pp. 79 and 80. On page 89 the total thickness of the upper and
middle Trenton limestone at Trenton Falls is given at 336 feet ; while on page 81 it is stated that the total thickness of the typical
Trenton Falls section is 318 feet 10 inches. However, in this latter place, if the sixteen feet in the zones repeated in the lower
part of the section be omitted, it will leave ten feet six inches instead of ‘ twenty-six feet six inches below D7” as stated by Mr.
White. In his later paper on “ The Original Trenton rocks *’ (American Journal of Science, Fourth Series, Vol. I, December,
1896, page 430) Mr. White gives 325 feet for the Trenton Falls section. Since the above was written I have received a letter
from Mr. White, in which he states that his section was thirty feet tov thick, because he mistook ‘a blurred 6” in his note

book fora 9. He further said that the following corrections should be made on pp. 78 and 79 of his article:
Total thickness,

‘ Feet.
* D12-13, a b : : ; J - : 4 S . é x é - : : 106
Di, ; : 4 : : 5 . ; 5 : 4 5 ; : n 5 " . : : 10814
D15 should read extending to the top of upper portion of High fall, ; * 5 A : p 168
D16, after third fall insert (Mill Dam fall), . “ ; 5 5 . 4 d : 5 4 5 182
DI7 (layer on which pier of R. R. bridge rests), . F y : é : i 5 o 6 7 5 185
pis, . “ 7 5 z 2 ° . c ; . . : ° 3 : 5 4 188
Diy, , ‘ ; : - 3 5 ; < ; . ; : : : ‘ = 2 E : 191
p20, ; ‘ 5 2 : é ; z c ; 5 : ; ¢ 3 A 3 : 198
D21, for Mill Dam read Alhambra, : ; 5 : 6 3 . | ‘ a 4 if x “ 199
p22, . é : ; 5 j : . : 2 ; A : 3 5 : - : : ; é 269
D3, 5 284

After making the above corrections it will be found that the rocks from the base of High fall to the top of Mill Dam fall
have nearly the same thickness in both sections, 186 feet in White’s, and 138 feet in that of Prosser and Cumings ©. s. P.

+ Thirteenth Annual Report State Geologist [New York], 1895, p. 425.
§ Second Annual Report Third District (Assembly Document, 1838, No. 200), p. 2%5.

NMOHS 3Yv¥ NOILOSS SHL SO gW GNV cW SSNO7Z ‘S1LYVd YSddN ANY YSMOT SHL HLO8 ONIMOHS ‘11v¥4 HOIH

ie 3

AM 31V Id +

ProssER AND Cumines—Lower SinuriaAn SEctTIons. * 627

vertical “with an average height of over one hundred feet,”’* and does not
give the thickness of the section. An earlier and quite accurate estimate was
made by James Renwick, who briefly described the geology in a paper read
in November, 1824, saying: “The river has worn itself a passage through the
rock for the distance of nearly two miles, forming a series of water-falls, and
has thus laid open to view the strata to a depth of probably 300 feet.”+

Tur Newrort SEcrIons.

In Newport township, some eight miles southeast of Trenton Falls, are
interesting exposures of the Calciferous sandstone, Birdseye and Black river
limestones. One of these is along the western bank of West Canada creek
and the cut of the Adirondack railroad, two miles above Newport village, and
one and one-half miles below Poland. At this locality the railroad is near
the bank of the creek and the cut is about 150 yards north of the fifteenth
mile-post. This section was described by Mr. White under the title of the
“ Poland lime kiln section, No. 130 A.” t

Section of the Newport Railroad Cut.

Along the bank of the creek and at the southern end of the railroad
cut is the following section :

STN BE Nearly opposite the fifteenth railroad mile-post, in P<
the bed of the creek and exposed about one foot above the level of the
water, is a heavy stratum of calcareous sandstone. The lithologic character
of this rock is like the Calciferous sandrock, to which formation it is referred.
An analysis of a specimen, from this stratum, by Mr. Edward P. McKeefe,
of Union College, gave the following result :

Si0, Speer rainy! calf het oe, 743% per eent.
et nee ert Se et fe AQ
OOO mr berth ex Pos A aS)
eo menseermrterrey 0), Ae? | ons, 1 2.98.

99.89 per cent.
?, Transitional layers from the Calciferous sandrock to the ,,¥°
Birdseye limestone. Thickness not accurately determined on account of the

high water. The upper six feet of this zone are composed of two layers of

impure limestone which are conspicuous in the lower half of the bank

* Geology of New York, Part IIT, 1842, p 52.
t Annals Lyceum Natural History, New York, Vol. I, Part I, 1824, p. 185.
$ Transactions New York Academy of Sciences, Vol. XV, April, 1896, pp. 82-84.

628 REpoRtT OF THE STATE GEOLOGIST.

below the railroad opposite the southern end of the cut. At high water
the base of this part is only about one foot above water level. Below are
thinner layers, shown a little farther down the creek, which are at least five
feet thick. Some of the layers in this zone are heavy and strongly arenaceous,
while others composed of a compact, dove-colored limestone, very similar to
the Birdseye, are quite conspicuous in the lower part. In some of the layers
are small Phytopsis-like tubes similar to the small ones in the Birdseye filled
with calcite. In one of the limestone layers near the bottom of this zone
are specimens of Leperditia which may be compared with the ostracoid
described by Professor Hall as Cytherina sp. from the Birdseye limestone of
Watertown, N. Y.* A sample from one of the limestone layers near the

bottom of this zone was analyzed by Mr. McKeefe with the following result:

S10, tcl. sed ee GAR ER a aia ln One aetenc eile
4) G “
FesQg oc 4bgai tes Sa a Re ee ee

Day) Splits. 6 APE ee tit et ee

MeCOy 275 Unk wee ere ee eee ene

100.80 per cent.
One of the arenaceous layers from the lower half of this zone gave the

following result :

SiO, er aN None Ap sh noah: 52.96 per cent.
FeO, ) cee ee ee ee
CaCOs. - 5° Gis Ce area SORT ele
MeCo, are ent ome 2.32 «

99.84 per cent.

DB. Birdseye limestone. For the most part somewhat thin layers o¢°%
of drab, very compact limestone with occasional quite massive layers. In
this rock are numerous specimens of what are considered small examples of
Phytopsis tubulosa, Hall, similar to those figured on Plate 8 (Figure Ne);
Pal. N. Y., Volume [. This limestone is well exposed in the railroad cut
and the creek bank below the southern end of the cut. Below the railroad
track at this place there is, at the bottom of the Birdseye, a vertical ledge six
feet thick of drab, typical Birdseye limestone. Near the base of this layer
the following fossils were found: Fafinesquina alternata (Con.), H. and C.;
Stictopora sp.; Leperditia sp.; and a gastropod. Next there are six feet,
one foot of which, perhaps, is covered; and in the railroad cut, nine feet

and six inches of typical Birdseye.

* Palaeontology of New York, Vol. I, p. 44, Plate X, Figure 12.

Prosser anD Cumines-—LoweEr Sinurian SEcrI0Ns.’ 629
L*. The upper part of the railroad cut is composed of a dark, ,F°*

» 1% = 41
irregular limestone, consisting of two prominent layers which, on weathering,

tend to separate into irregular layers and these in turn to break into lumpy

masses. The rock weathers to a grey color and in the railroad cut seven feet
and two inches are shown; — Black river limestone.

SECTION OF CUT
WORTH OF NEWPORT
No. 49,2.

=a 70° of Cur

Bath fiver

BIN OSEVE

Wa Rusk nae Sous war ARENACE OVS
ore

Mi) Lavea of Binosé va

2/9” rie CL ET YE

=e —< FAIL ROAL
Serer
Gin OSEYVE a
me
t uf
1°
yt
Pewee ter wees ewe see ee teeta vi
D
BIROSE VE ‘

TRANSITIONAL
! aft
~~ eee wee ee we ew ee we ee a shot
mate
VL
s’ Gort wlan
TRANSITIONAL BIROSE YE (2) Ant Ee
angers
oe 3 —
Me iw-eore mee eww ew we wee ee eee ee eee ee
Be ZZ 2 Canc FEROUS

B. Covered between the top of the railroad cut and the fb
highway.
Bs

In the bank above the highway, near the old lime-kiln, is dark
blue, thin-bedded, fossiliferous limestone, with shaly partings, contaming

abundant Trenton fossils — Trenton limestone.

630 Report oF THE STATE GEOLOGIST.

At the northern end of the railroad cut west of the track is the following
section :

No. 1. Mixed drab Birdseye limestone and slate-colored, impure [°%
limestone. A little farther down the track all this zone will be found to
have changed to the typical Birdseye limestone. This shows the variation in
the lithologic character of the Birdseye when followed only a short distance.

Jo. 2. Massive layer of somewhat impure Birdseye limestone Ff iz _¥*
from one foot to one foot and four inches thick. Vertical tubes similar to
those in the more typical Birdseye. This layer forms the top of the Birdseye
in Mr. White’s section.

No. 3. Clear, bluish-drab, typical Birdseye limestone in two ¥_ iin,
layers.

No. 4. Black river limestone. Dark, bluish-black, fine grained ¥_ 7;
and lumpy, weathering to a grey mottled with blackish spots. Very distinct
line between the base of the Black river limestone and the Birdseye.

It will be noticed that the above sections do not agree closely with that
described by Mr. White. The greater part, if not all, of the eight feet
referred by White* to the Calciferous formation is in the zone which has
been called, in this paper, transitional from the Calciferous to the Birdseye.
Apparently, the ledge of Birdseye limestone below the railroad was not
noticed by White, for it is stated that the ten feet between the top of the
so-called Calciferous and the base of the Birdseye on the west of the railroad
cut is covered by debris. In the railroad cut Mr. White drew the line of
division between the Birdseye and Black river limestones through the
Birdseye limestone at the top of No. 2 of our section, at the northern end of
the cut. White described this stratum, which may be traced for the entire
length of the cut, as “a bed one foot thick, somewhat crushed on the
surface, which weathers yellow.” However, there are five feet of typical
Birdseye above this layer which White referred to the Black river limestone
as No. 6 of his section and described as “two heavy barren beds of dark
colored, compact limestone, five feet” in thickness. When these beds are
referred to the Birdseye limestone its thickness 1s ten feet and ten inches at
the northern end of the cut, and nine feet and six inches at the southern end
instead of five and one-half feet, as stated in his section. Nos. 7 and 8 of
White’s section belong in the Black river limestone, for which he gaye a

thickness of six feet and nine inches.

* Op. cit., p. 82.

ProssER AND Cumincs—Lowerr SILURIAN SECTIONS. - 631

Section of the Moshier Quarry.

About one-half mile north of Newport is an extensive quarry known
as the Moshier, in which both the Birdseye and Black river limestones are
quarried,

XLILIX A’. The Calciferous sandrock is shown in a railroad cut near
the Newport station and it may also be seen at various places in the
field between the cut and the quarry. Only the upper part of the formation
is shown, however, and its thickness was not determined.

A*, Compact, drab limestone in the lower part of the Moshier ,***
quarry, at its northern end and near the railroad level. The rock is similar
to the typical Birdseye limestone to which it is referred. The contact
between the Calciferous sandrock and the Birdseye limestone not shown.

A’, An arenaceous stratum from ten inches to one foot thick, Fe
which splits into layers from two to three inches in thickness. Somewhat
like the Fucoidal subformation of the Calciferous.

A‘, Typical drab-colored Birdseye limestone extending to the top g5/""as
of the lower quarry.

A®, Partly covered Birdseye between the lower and upper ; "ti,
quarries,

A’. Massive Birdseye limestone forming the lower half of the ; *%,,
western wall of the upper quarry. It is a drab, compact rock that weathers
to a light grey and splits into layers that are thinner than those in the Mohawk
valley. This is the top of the Birdseye and the line of division between it
and the Black river limestone is beautifully shown in the eastern and
southern parts of the quarry.

A‘, The Black river limestone, bluish-grey, breaking into lumpy 5,.°°Sa,
blocks, is composed of two massive layers in the Moshier quarry, the lower
two feet and six inches and the upper three feet thick. The following fossils
were collected :

1. Monticulipora (Prasopora) lycoperdon (Say). (c)
2. Columnaria alveolata, Goldt. (c)
3. Rafinesquina alternata (Con.), Hall and Clarke. (c)
4. Cypricardites cf. obtusus, Hall. (r)
5. (2) Nucula levata, Hall. (r)
6. Laphistoma cf. americana, Bill. (r)
7. Leperditia fabulites, Con. (7)
8. Asaphus platycephalus, Stokes. (1)
9. Streptelasma cf. profunda, Hall. (1)

632 Report OF THE STATE GEOLOGIST.

In a ledge a short distance southeast of the Moshier quarry is an
exposure of ten and one half feet of Birdseye limestone. From this ledge and
the upper part of the Moshier quarry the following species were collected :

1. Phytopsis tubulosa, Hall. (c)
Small specimens similar to figures 1, 1c, Pl. 8, Pal. N. Y., Vol. L.
2. Murchisonia ef. varicosa, Hall. (1)
3. Orthoceras multicameratum, Con. (c)
4. Modiolopsis sp. (1)

5. Rafinesquina alternata (Con.), Hall and Clarke. (c)
6. Leperditia sp.
A specimen from the upper part of the Birdseye limestone at this
locality was analyzed by Mr. McKeefe, with the following result :
LO Al ae eae a PRES Co eee rs le a bo ZL NOS ORNS,
jen @ WER PEI PME IgE ok LP a Pe all
CaCQg. > Foe ee a rie een Ot
Me COs os SCSI 3 2 See Ee ee ne eae ere la

100.95 per cent.

All of the limestone shown in the lower part of the Moshier quarry is
considered as belonging in the Birdseye, which gives the subformation at this
locality a thickness of at least twenty-two and three-quarters feet. Emmons
stated that the thickness of the Birdseye to the northwest in Jefferson

county, was “not far from thirty feet.”*

Litrné Fats.

Thirteen miles southeast of Newport in the Mohawk valley, is Little
Falls, a locality famous alike for its natural scenery and geologic structure.
The section is introduced here in order to give the thickness of the Caleif-
erous sandrock and to show the decrease in thickness of the Trenton
limestone as compared with that at Trenton Falls, only twenty-two miles
to the northwest. At this place is the upper gorge of the Mohawk river,
where the falls and the lower part of the cliffs are composed principally of
gneiss, which has generally been referred to the Laurentian system of the
Archaean. The gneiss is excellently exposed in the cliffs on the northern
side of the river along the tracks of the New York Central railroad, in the
eastern part of the city, as may be seen in Plate VI. Above the gneiss are
steep walls of Calciferous sandrock which are especially conspicuous on the

southern side of the river opposite the railway stations.

* Geology of New York, Part IT, 1842, p. 385.

"LSVa ONINMOOT '13auLS
3HL SAOSV ANOLSGNVS SNOYSSIOIVD JO 3dINO ! SSISND NVILNSYNY] HONOYHL ‘SIV4 SILLIT LV LNO Gvowtivey SYOHS 1Sa/\\

Tah

a ae

Foo GuoIMvyo NaBeNa Iv dOON

A 31V1d"

‘
om

Prosser AnD Cuminas—Lower SILuRIAN SECTIONS. 633

Section Northeast of Little Falls.

The following section begins at the river level below the falls in the
eastern part of Little Falls and continues northerly for about two miles,
nearly to the summit of the general elevation for that region.

XLVII B. The Laurentian rocks composed principally of 96%%3
gneiss have a thickness of 203 feet as determined by tape and Locke level
measurements. The barometric readings gave 200 feet of the gneiss and
this part of the section may be divided as follows: From the river to the
New York Central railroad, forty feet of garnetiferous gneiss, the base of
which is well exposed along the river; vertical cliff of thirty-three feet of
similar gneiss, weathering to a reddish-brown, to level of Little Falls and
Dolgeville railroad; gneiss forming cliff above Little Falls and Dolgeville
‘ailroad, including the conspicuous layers above the cut, sixty feet; gneiss in
the cedar grove where the joint openings are conspicuous, then mostly covered,
but exposed near the top just below Loomis street, seventy feet. All the
gneiss except the seventy feet of the upper part is well shown in Plate
VII, which is a near view, looking westward, of the gneiss along the
New York Central railroad in the eastern part of Little Falls.

L”. In the base of the Hiram Boyer quarry on Loomis street, Just "Sy
above the gneiss, is a very coarse-grained, quartzitic sandstone containing
quite large quartz pebbles. At present the contact of this sandstone and
the gneiss is hardly shown, though Mr. Boyer states that in the deeper part
of the quarry, former excavations showed it very distinctly. In general, the
gneiss apparently dips heavily to the northeast, while in the quarry the
sandstone has a dip of from one to one and one-half degrees to the north-
west. Professors Shaler and H. 8. Willams studied this exposure some
years ago and, it is believed, determined that the sandstone rests uncon-
formably upon the gneiss.* Mr. Walcott stated that this sandstone “ has
been referred to the Potsdam,”+ though he apparently did not accept this
correlation, for he said: “it is doubtful if we can claim the presence of the
Potsdam at any point in the Mchawk Valley.”

L*®. Bluish-black, finely arenaceous shale, nine inches thick, ,"°%,
weathering to irregular pieces. It contains fairly well preserved specimens of
Lingulepis acuminata, Con., which were first discovered by Professors
Shaler and H. 8. Willams, and reported by the latter at the Washington
meeting of the Geological Society of America, in 1890.

*See Walcott : Correlation Papers—Cambrian. Bulletin United States Geological Survey, No. 81, pp. 207-347.
+Ibid., p. 347.

‘a tThid., pp. 207, 347. The paper has never been published, but its title occurs on p 634, Vol. 2, Builetin Geological Society of
merica

§34 Report OF THE STATE GEOLOGIST.

SECTION FROM
WVCKHRRR GOT TO
TOP OF HILL

NORTHEAST OF LITTLE FALLS

No.#7, B,
ER Com ‘ ngs.
a7 Se oe frei) 2 Ser eee
; Utica.
eft 2 - _-----------------~-------------. Br
| SN
He ieee of Trenton. Terie
97’ ZZ Be
676). __
124,
Mee SS SS SS a ee Birdseye.
Bs
16S
. 494 = Thin layers.
FIGS” a Ledge in field.
8’
Zp Calciferous.
Zm &
ZOLA Foe ie eS a ee et Le ee <
776’
aa | per ae IO Cs pe es EY Top of cut.
bé(
Wea DL StS RAT EETE Ste Shale. @s

Conglomerate. Ba

AO MOY YAddN SO WOVE SNOLSONVS SNOYSAINIVD AO 3SVG ‘STW-| AILLI]
JO MAIA QHVMLSV3 WYAN3*)

‘QVONTIVY IWYLNSD MYO, MAN SHL DONOW SSISNO NVILNSYNV]

YW
I

JO LuVd NYS1SVS =
= , |
“e OD AGYOIMVYO HOSENAVIWH dOOMNAM
walt ¢ ~ t

An
¥ ’
; v

IA ALW1

Prosser anp Cumrncs—Lower SriurRIAN SEcrTIONS. _ 635

L*. Above the shale is the massive Calciferous sandrock, seventy- 46°%bo
four feet of which is exposed in the wall of the quarry. This part of the for-
mation is composed principally of compact, thick-bedded, greyish calcareous
sandstone that has been quarried. In the lower part are occasional shaly
partings, similar to B*, but no fossils were found in them. This quarry is
shown in Plate VIII, where Mr. Birch stands on what is said to be the top
of the gneiss, the two heavy layers at the base of the cliff being the sandstone
of B®; the stratum of fossiliferous shale is marked by the hammer, while
above is the massive Calciferous sandstone.

In the fields above the Boyer quarry the rocks are partly covered, yet
there are sufficient exposures to make possible the determination of the top
of the Calciferous. In the upper part it is thinner bedded than in the lower.
No fossils were found.

L*, On the Ritter farm, near the house, is a ledge composed of 52°64
thin layers of compact, fine-grained, dove-colored limestone, containing vertical
tubules filled with calcite similar to the small ones found near Newport and
referred to Phytopsis. The thickness is approximately five feet and it is
referred to the Birdseye limestone.

B®. For fifty-three feet above the Birdseye the rocks are covered, of °°%¢g
when a ledge of Trenton limestone, five feet thick, appears. The rock is a
crystalline greyish limestone and contains an abundance of Trenton brachio-
pods. Above this ledge forty-six feet are covered before the base of the black
shale is reached; but it is probable that nearly if not all of this 104 feet
belongs in the Trenton. The following species were obtained from the five-
foot stratum:

1. Rajinesquina alternata (Con.), Hall and Clarke. — (aa)
2. Plectambonites sericea (Sowb.), H. and C. (a)
3. Orthis (Dalmanella) testudinaria, Dal. (c)
4, Monticulipora (Prasopora) lycoperdon (Say). (a)
5. Calymene callicephala, Green. (1')
6. Asaphus platycephalus, Stokes. (1)
7. Orthis (Dinorthis) pectinella (Kmm.), Hall. (7)
8. Orthoceras sp.
9. Zygospira recurvirostra, Hall. (1°)
10. Trinucleus concentricus (Eaton), Hall.
11. Escharopora recta, Hall. (7)

")

12. Crinoid segments.

636 Report oF THE STATE GEOLOGIST.

LL. Black carbonaceous shale at the base of the Utica formation; ,,"°,
nineteen feet exposed on the hill near the Eysaman house.*

Vanuxem, in describing the rocks about Little Falls, states that “the
gneiss rises at the east end to the height of a hundred feet,” while the Cal-
ciferous is given as having “a thickness of over 200 feet.” + In each case it
will be noticed that the thickness is more than twice as much as Vanuxem’s
estimate. Darton gave the thickness of the Calciferous as from “200 to 250
feet on the Mohawk,” } while the Birdseye is mentioned as having a thickness
of “four feet about Little Falls.”§ On the south side of the east and west
road west of the Eysaman house is an old quarry and lime-kiln, known as the
Cook quarry, in which the contact of the Birdseye and the Trenton limestones

is clearly shown.

Section of the Cook Quarry.

XL VII C*. Fine-grained, dove-colored Birdseye limestone. In gf*%hy
the lower part of the quarry are exposed four and one-half feet, composed of
the three following layers in ascending order: two feet and three inches, one
foot and. five inches, and nine inches. The vertical, small P/hytopsis markings
were present, but no other fossils.

C*. Thin, irregular layers of dark-colored Trenton limestone 44°" ;,
somewhat crystalline and highly fossiliferous; twelve and one-half feet are

exposed in the quarry wall.

1. Orthis (Dalmanella) testudinaria, Dal. (aa)
2. Orthis (Dinorthis) pectinella (EKmm.), Hall and Clarke. — (ce)
3. Rafinesquina alternata (Con.), H. and C. (1)
4. Plectambonites sericea (Sowhb.), H. and C. (c)
5. Asuphus platycephalus, Stokes. (1)
6. Stictopora ct. acuta, Hall. (1)
7. Monticulipora (Prasopora) lycoperdon, (Say). (1)

8. Crinoid segments.

On the south side of the river opposite the central part of the city is a
nearly perpendicular cliff of massive Calciferous sandrock, 300 feet in height.
About 170 feet above the base is a four-foot stratum containing specimens
apparently of Cryptozion proliferum, Hall. Below the Calciferous sandrock

is the gneiss which is excellently shown in the West Shore railroad cut east

* Recently Mr. M. L. Haviland and other students of Union College, measured the section north of Little Falls. They
obtained a thickness of 217 feet for the Laurentian gneiss ; 446 feet for the Calciferous; 81 for the Trenton, and 27 feet of Utica
slate to the top of the hill. c.s8 P.

t Geology of New York, Part III , 1842, p, 209. For the thickness of the Calciferous, see also p. 82.

+ Thirteenth Annual Report State Geologist [New York], 1894, p. 418.

§ Ihid., p, 422.

“1S3M SNIMOO7] ‘S11V4 311117 LV SSIAND NVILNSYNV] SO 45110 SHL SO MGSIA ysayvaNn

OO OHOAMWYS MOFENATIVH GOOMNAM

WA 3Lvid

7

t
Pp

fs
bia A
a

Arak

, ‘
ae ee.) er Pi

ProssER AND Cuminecs—Lower SinurtAn SEcrIoNs. ~ 637

of the station. Plate IX gives a view of this locality, looking eastward,
the cut being through the gneiss, and the cliff above the street being com-

posed of the lower part of the Calciferous sandrock.

CANAJOHARIE AND PALATINE BRIDGE.

Along the Mohawk river on both the north and south sides, in the
vicinity of Canajoharie, are numerous outcrops of the Calciferous sandrock.
The exposures are in the upper part of the formation and belong in the
substage which was named the Fucoidal layers by Vanuxem,* who stated

that the best exposition of these layers “ was at Canajoharie.”
) J

Shaper Quarry.

In the western part of Canajoharie village is the Shaper quarry, which
is extensively worked, exposing some forty-four feet of the Fucoidal layers.
The following section from the level of the West Shore railroad to the top
of the quarry gives the thickness of the different layers as exposed in this
quarry : '

No. 15. Soil on top of quarry.

14. 3 feet, 9 inches.

TSrenneeehysas

Loy 32-5

DAN e eae ED a

WO Wen

Vr Da ne eae

Sethe (Not fucoidal.)

(ieee Se Spal Mae (Not fucoidal. )

(SON Se eae ied (Fucoidal markings very conspicuous.)

Doping Gcba

JC ee ee (The top of this layer forms the floor of the

middle part of the quarry and is its
main ledge.)

Drea o

een Omen (Lowest layer in the quarry.)

IAD AO oat (From the bottom of the quarry to the

level of the West Shore railroad.)
The above section gives a thickness of forty feet and four inches of

Calciferous sandrock in the quarry, or a total of sixty feet and four inches

* Fourth Annual Report Geological Survey of the Third District [New York] (Assembly Document No. 50, 1840), p. 369.
} Geology of New York, Part III, 1842, p. 87.

638 Report OF THE STATE GEOLOGIST.

for the section from the level of the West Shore railroad below the quarry
to its top. The dip is about sixty degrees west of south and the amount
varies from four to eight degrees in the different portions. This quarry was

described some ten years ago by Professor Smock.*

Canajoharie Creek Section.

The Canajoharie creek flows through the central part of the village, and
exposures of the Calciferous sandrock begin along its sides opposite Arkell
& Smith’s paper bag factory. Along this part of the creek the banks are
not steep, but about one-half mile farther up the stream they become steep
and in places there are vertical rock cliffs, seventy-five feet or more in height.
Near the lower end of this gorge the Calciferous passes beneath the bed
of the creek and is succeeded by seventeen feet of thin bedded Trenton
limestone, above which is the Utica slate forming the cliffs of the greater
part of the glen. In describing this region Mr. Darton stated that in
descending the Mohawk river the thickness of the Trenton limestone
gradually decreases until at Canajoharie “the amount is only six feet,”
and further says, “the formation is well exposed on the creek behind
Canajoharie.”+ In the upper part of the gorge the older rocks are covered
by a deposit of boulder clay, which in places has a thickness of some
seventy-five feet.

LIT GB. Fucoidal substage of the Calciferous sandrock from ,f&t,
the base of the Trenton to the level of the West Shore railroad. The lowest
exposures noted are on the bank of the creek opposite the Arkell & Smith
factory above the West Shore railroad bridge, and about on a level with
the track.

?. Thin-bedded dark blue, very fossiliferous Trenton limestone, ,7°4,
separated by shaly partings, with a total thickness varying from sixteen to
seventeen feet, as measured on the vertical banks of the creek. The line of
division between the Trenton and Calciferous formations in this section is
clearly shown, for the upper part of the Calciferous is slightly flexed and
upon it the regular layers of the Trenton rest. This shows a slight folding
of the Calciferous previous to the deposition of the Trenton and indicates
between them a time break of considerable duration which, in northeastern
New York, is filled by the Chazy limestone. Darton gave a picture of the

creek bank, showing the contact of the Calciferous and Trenton.

* Builetin New York State Museum , No. 3, 1888, pp. 109-110. See ibid., Vol. 2, No. 10, 1890, p. 245.
+ Thirteenth Annual Report State Geologist [New York], 1894, p. 425.
¢ Ibid., pl. 5.

‘YSINWVH AS GSLVOIGNI SqVHS VINSON) “ANOLSONVS SNOYSSIONVD NI AYYWNd ysAog

OO GXOAMVY'D MOSSNa aH SOON AM

IIA aLW1d

Prosser: AND Cumrincs—Lowerr SILuRIAN SEcrIoNsS. 639

B®. Very black, bituminous Utica slate forming the greater part 39)°%"320

of the walls of the glen. It is quite calcareous and more fossiliferous than

‘that in the exposures farther down the Mohawk valley, and the exposure of

fully 300 feet in the gorge belongs in the lower part of the Utica formation,
In the lower part of the gorge is a fall over Utica slate, the top of which is
about forty-five feet above the base of the slate. This locality was cited by
Mr. Darton as “one of the finest exposures [of Utica slate] in the Mohawk
valley,” and a picture of the falls was given in his report.*
The thin layers of Trenton limestone in the Canajoharie gorge are abun-

Loy
(S)

dantly fossiliferous and: the following species were collected :

1. Rafinesquina alternata (Con.), Hall and Clarke. (c)
2. Calymene callicephala, Green (?). (r)
3. Orthis (Dalmanella) testudinaria, Dal. (a)
4. Asaphus platycephalus, Stokes. (c)
5. Monticulipora (Prasopora) lycoperdon, Say. (1)
6. Modiolopsis mytiloides, Hall (?). (rr)
7. Tellinomya levata, Hall. (11)
8. Zygospira recurvirostra (Hall), Winch. and Schuch. (rr)
9. Plectambonites sericea (Sowb.), H. and C. (c)
10. Trinucleus concentricus, Eaton. (7)
js Atrypa (Protozyga) exiqua, Hall. (r)
12. Ceraurus pleurexanthemus, Green (2). (ar)
13. Murchisonia bellicincta, Hall. (rr)
14. Murchisonia gracilis, Hall (2). (7r)
15. Camarella ef. Volborthi, Bill. (rr)
16. Stictopora sp. (r)

As already stated, the Utica slate contains a larger number of fossils
than has been found in the more eastern exposures. The list is as follojvs,

and it undoubtedly might be materially increased by further search.

1. Lingula quadrata (Kich.), Hall (2). (c)
2. Plectambonites sericea (Sowb.), H. and ©. (a)
3. Orthis (Dalmanella) testudinaria, Dal. (c)
4. Triarthrus Becki, Green. (c)
5. Graptolites. (a)
6. Asaphus platycephalus, Stokes. (r)
7. Tellinomya nuculiformis, Hall. (1)

* 1bid., p. 429, pl. 7.

640 Report OF THE STATE GEOLOGIST.:

8. Pterinea Trentonensis (Conrad). (rr)

9. (2) Edmondia subtruncata (Hall). (rr)
10. Hndoceras proteiforme, Hall. (c)
11. Raphistoma lenticulare (mmons). (1)
12. Trocholites ammonius, Conrad. (1)
13. Rafinesquina alternata (Con.), H. and C. (r)
14. Orthis (Dinorthis) pectinella, Etam., var. semiovalis, Hall. (rr)
15. Crinoid segment. (rr)
16. Leptobolus insignis, Hall. (r)
17. Lingula curta, Con. (a)
18. Monticulipora (Prasopora) lycoperdon, Say. (17)
19. Bellerophon sp. (rr)

The Mohawk Valley Stone Company’s Quarry.

On the northern side of the Mohawk river to the west of Palatine
Bridge is the extensive quarry of the Mohawk Valley Stone Company,
formerly called the Frey. This quarry is in the Fucoidal substage of the
Calciferous and in recent years a large amount of stone has been shipped
from it. At present it is, probably, the most largely worked quarry in the
Mohawk valley. On the upper surface of the rock, near its eastern end,
are glacial striae.

LIT ©. Covered from the level of the New York Central rail- ,Fet,
road track to the base of the quarry.

Cc? The lower half of the quarry, consisting of fucoidal Caleif- ,°%,
erous sandrock which splits into three prominent layers that become thinner
on the weathered surface and thus do not extend for any considerable
distance,

C*, Nine feet and four inches of fucoidal Calciferous sandrock, ,F°¢,
in fairly thick layers, forming the upper part of the quarry.

In the field to the northeast of the quarry a ledge of Calciterous rock
was noticed, but no other formation was seen below the highway. Mr. Darton
stated that the Fucoidal beds in the vicinity of Canajoharie, “have a
thickness of about ten feet and le about six feet below the top of the
formation.” It is perfectly evident after an examination of the quarries on
either side of the Mohawk river at Canajoharie, that the thickness of the

Fucoidal substage is much greater than ten feet.

* Thirteenth Annual Report of the State Geologist [New York], p. 421.

Lu

NOILOSS SHL SO 6¢V GNV eV SANOZ ‘SS5I190 SHL SO LYVd YaddN SHL
-SINIT SNITIVLSAYS SAISSVN SHIL

NI NAAOHS SI SNOLS
390INe GVONTIVY AHOVGNONIGY SHL 3AOSV WaaHO VGYNYD 1S3M\ 4O AGIS 1sva SH1 NO 449

X! 3LW1d

me 2

‘
4 ee

ProssER AND Cumincs—Lower SILuRIAN SECTIONS. ° 641

SPRAKERS.

Twenty miles southeast of Little Falls and three miles below Canajoharie

ds the small village of Sprakers,* at the upper end of the lower gorge of the

Mohawk river. About a mile below the railroad stations the valley is very
narrow and is bounded on each side by nearly perpendicular walls, in places
350 feet in height, composed largely of Calciferous sandrock. About two
miles below the New York Central railroad station, on the northern side of
the river, is a conspicuous pot known as the Great Nose, where the
Laurentian gneiss is exposed, above which the massive Calciferous sand-
stone is clearly shown. On the southern side of the river opposite this
point and farther down the river in the valley and in the West Shore railroad
cuts at the foot of Little Nose, the gneiss is also shown. The scenery in
this gorge is very picturesque and the locality is one of the most charming

in the beautiful Mohawk valley.

Flat Creek Section.

At Sprakers, Flat creek enters the Mohawk river from the south, the
banks along its lower course being steep and rocky. From the village to a
point a short distance above the falls, the rocks along the creek belong to the
Calciferous sandrock, while the bank above shows about seventeen feet of
Trenton Imestone, capped by Utica slate. A quarter of a mile farther up
the creek the second gorge begins, the steep sides of which are composed
entirely of Utica slate. At least 230 feet of the slate are shown in the
bank of the creek. There is a fall formed by some of the harder layers of
the slate, while pillars of erosion and several very pretty amphitheaters
occur.

VII A*. Covered slope from the river level to the lowest
rocks exposed in Flat creek.

A*, Light grey, massive, calcareous sandstone exposed in the ,,"et,
creek bed and along its steep banks. Calciferous sandrock,

A’. In the upper part of the Calciferous, a portion of the layers ,,"°%,,
is thinner and contains great numbers of fucoidal markings. There is no
sharp line of division, but these fucoidal layers begin to be conspicuous some
ninety-five feet below the top of the Calciferous. In the upper part of the
fall, about one mile south of Sprakers, are thick strata similar to those quar-

ried at various localities in the Mohawk valley termed the “* Fucoidal layers,”

*On most of the maps this village is called Sprakers Basin, but Sprakers is the name of the post office and of the railroad

Stations.
41

642 Report oF THE STATE GEOLOGIST.

by Vanuxem. The statement that these massive fucoidal layers are from ten
to fifteen feet in thickness and confined to the upper twenty-five feet of the
formation is misleading, for layers of similar structure and appearance occur
along the Mohawk valley at least 130 feet below the top of the formation.
In a quarry on the east side of the creek, near the top of the bank, are layers
of the massive fucoidal limestone containing specimens of Ophileta compla-
nata, Van.

A‘ Thin layers of dark blue, fossiliferous limestone, well exposed 4°39
in the steep bank above the fall and highway bridge, from sixteen and one
half to seventeen feet in thickness. Trenton limestone.

A’. Very black, argillaceous shale which forms the steep banks 9542 tig,
of the creek in the second gorge. Utica slate. ‘The 230 feet do not represent
the thickness of the formation in this region, but should be considered to
refer simply to its lower part which is admirably exposed in this gorge.

The above section is important from the fact that it shows the thinning
of the Trenton formation from an approximate thickness of 109 feet at Little
Falls, twenty miles northwest, to about seventeen feet in Flat creek.
Furthermore both the Birdseye and Black river limestones are wanting. The
dip varies from 5° to 7°, N. 84° W. along the lower gorge.

Some ten years ago, a diagrammatic section of this creek was published,
which represented the Calciferous, Chazy, Trenton and Utica formations.*
The thickness of the Trenton limestone is given as “from ten to fifteen feet,”’+
which is the only measurement recorded, and the Chazy limestone appears

not to be present.

West Shore Railroad Cut Section.

About one and one-fourth miles below Sprakers is the West Shore rail-
road cut, with a nearly perpendicular southern wall of Calciferous sandrock
which reaches a height of 350 feet.

VIT B. Top of the Laurentian gneiss, exposed at the eastern end
of the cut.

>, Basal part of Calciferous sandrock extending from the top 43°;
of the gneiss, 1,500 feet along the side of the railroad to the point where the
nearly vertical cliff of Caleiferous was measured. The thickness is estimated
from the dip which is about 1°, N. 85° W.

33. From the railroad level to the brow of the cliff forming the 36 °%sg5
nearly perpendicular wall of the railroad cut. The cliff is composed entirely

* Fifth Annual Report of the State Geologist [New York], 1886, p. 9.
+ Ibid., p. 8.

‘ANOLSONVS SNOYSSIOIVD SHL YSAO ‘SYSBYVHdS ‘MASH 1vI4 NI STIV4

9 youve wa 1whidoos ie eatin - : : ; 3 ea rr
tk ea pike , 2 aS. v4

“e.. : % Ss ; %
i ; ¢

X 3Lv1d

ProssER AND Cumincs—Lower Simurtan SEctrions. 643

of the massive, light grey Calciferous sandrock and is one o1 the best out-
crops of the formation to be found in the Mohawk valley. A specimen of
- Cryptozobn proliferum, Hall, was found near the middle of the cliff.

B+. In the field south of the cliff, mostly covered, showing only ¢5"°"s
occasional outcrops of the Calciferous sandrock with a conspicuous stratum
at the top of the first terrace south of the cliff.

B®. Partly covered, still showing plenty of outcrops of an arena- 4"°%fo
ceous, compact, greyish rock with irregular fucoidal markings. Several
specimens of Ophileta complanata, Van., and also the form named QO. /evata
by Vanuxem*, have been found in the somewhat shaly layers of this division.
The Calciferous sandrock caps the highest land about one mile southwest of
the railroad cliff, although it is undoubtedly near the summit of the
formation.

The above section shows that the Calciferous formation has a thickness
of 500 feet in the region of Sprakers and the lower gorge of the Mohawk
river. This decided increase over the supposed thickness will be appreciated
when it is stated that Vanuxem gave it as “ upwards of 200 feet thick at the
Noses and Little Falls.”+ Darton states that ‘“ the formation has a thickness
of 200 to 250 feet on the Mohawk, and the amount appears to be constant
over a wide area.”{ The thickness of the Calciferous sandrock along the
Mohawk valley is thus shown to be 500 feet which is some 250 to 300 feet

greater than has generally been given.

Section at Yosts.

On the northern side of the Mohawk river at Yosts, three miles below
Sprakers and five miles above Fonda, is a high and steep cliff composed of
the Calciferous sandrock. This locality is at the eastern end of the lower
gorge of the Mohawk river and the massive, nearly horizontal layers of the
Calciferous formation are conspicuously visible from the trains of the New
York Central railroad. (See Plate 1.)

VI ©’. Covered from the railroad track to the base of the cliff. ,,Fe',,
The greater part if not all of this covered division belongs in the Calciferous.

O*, Massive layers of Calciferous sandrock, forming the nearly 4»,
perpendicular cliff. From the base of the Calciferous ledges to the brow of

the cliff.

* This species is referred to O. complanata by Whitfield. See Bulletin American Museum of Natural History, Vol. II, p. 49

+ Geology of New York, Part III, p. 32. On p. 205 Vanuxem stated that the Calciferous cliff at the Noses ‘rises vertically to
two hundred and more feet.”

¢ Thirteenth Annual Report of the State Geologist [New York], p. 418.

644 Report oF THE STaTE GEOLOGIST.

C*%. From the brow of the cliff to the top of the bill, Partly j5¢°"%S5ss
covered but showing ledges of Calciferous sandrock to the top of the hill.

The Calciferous sandrock forms the top of this hill and no indication of
the Trenton was found. The Fonda sheet of the United States topographic
map shows that the difference in altitude between the New York Central
railroad and the top of this hill is between 560 and 580 feet. This section
shows at least 450 feet of Calciferous sandrock to which, probably, the greater
part if not all of the covered 112 feet at the base of the section should be
added, which would indicate a thickness of more than 500 feet of Calciferous.

Tries Hi anp Forr Hunter.

North Side of the Mohawk.

Tribes Hill is a small village about half way between Fonda and Amster-
dam, and opposite the mouth of the Schoharie creek, which enters the
Mohawk river from-the south. The Trenton limestone is exposed on both
sides of the Mohawk at this locality, the most extensive outcrop being in the
quarry below the railroad and the cut above it Just west of the Tribes Hill
station. The section of this quarry and railroad cut is as follows:

XLIIV <A*. Compact, dove-colored limestone, with smooth fracture,
weathering to an ash-grey color. The basal layer m the eastern part of the
quarry ; its contact with the underlying rock not shown. Birdseye limestone.

A®. One or two layers of very lumpy, fine-grained blackish lime. 2%
stone with small, sparkling crystals of calcite. Very few fossils; now and
then a specimen of Pafinesquina alternata (Con.), H. and C., and Strep-
telasma sp. This zone is doubtfully referred to the Black river limestone.

A®, Massive, dark blue limestone, mostly fine-grained but with ,7%t;
crystalline layers which usually contain some fossils, Streptelasma being the
most abundant. In the eastern end of the quarry the limestone has almost
the appearance of a single layer, though it divides along several indistinct
bedding planes. Trenton limestone.

A‘, Varies from thin, very unevenly bedded greyish, crystalline ,f%%,
to dark-colored, highly fossiliferous limestone. Lower part appears as a thick
layer when freshly opened.

A’. Thin-bedded, uneven, dark-blue limestone in the railroad cut Ft,
above the quarry. Trenton.

The dip varies in different parts of this exposure as, for example, in one
part of the quarry it is 54°, S. 45° W., and in the railroad cut 4°, S. 50° W.

‘“ONINMOG JO LSAM 'LND GvVONTIVY SYOHS 1ISA/\ NI SNOLSGNVS SNOYSIIOWVD JO gsvq

IX 31V1d

Prosser AND Cuminas—LoweEr SILURIAN SxKcrrons. 645

On the river bank a little west of the quarry and apparently forming the
bottom of the river is the top of the Calciferous sandrock.
From the thin-bedded Trenton limestone of A‘ the following species

were collected :

1. Plectambonites sericea (Sowb.), H. and C. (aa)
2. Orthis (Dalmanella) testudinaria, Dal. (aa)
3. Orthis (Dinorthis) pectinella, Emm. (c)
4. Escharapora recta, Hall (?). (Ge)
5. Stictopora acuta, Hall (?). (1r)
6. Stictopora elegantula, Fall. (rr)
7. Asaphus platycephalus, Stokes. (c)
8. Ceraurus pleurecanthemus, Green. (1)
9. Lafinesquina alternata (Con.), H. and C. (a)
10. Leperditia fabulites, Con. (c)
11. Rhynchotrema capax (Con.), H. and C. (c)
12. Murchisonia gracilis, Hall. (c)
13. Murchisonia bellicincta, Hall. (c)
14. Raphistoma lenticulare, Emm. (c)
15. Endoceras proteiforme, Hall. (r)
16. Schizocrinus nodosus, Hall. (c)
17. Modiolopsis mytiloides, Hall (2). (ar)

On the upper side of the railroad, a short distance east of the Tribes
Hill station, is a large quarry in the upper part of the Calciferous formation.
The section from the base to the top is as follows:

XLIIV LB". Compact, blue, somewhat “ fucoidal” limestone. arg bg

SL, Dark grey, non-fucoidal limestone in one to three layers, 3",
showing yellow streaks on weathered surface.

B®, Massive drab to light grey limestone in one or two heavy ,f**,
layers. Weathered surface finely mottled by horizontal streaks. Fucoidal
limestone.

L*. Strongly fucoidal massive beds of bluish-grey color, capped 43°,
by a dark blue thin layer containing Ophileta complanata, Van.

BB. Medium thick beds of arenaceous limestone which weathers f°,
to a buff.

B’. Two layers of Calciferous immediately back of the crest of ,*°t,
the quarry.

The entire quarry is composed of Calciferous sandrock, though there is a

four-inch layer Birdseye limestone just above it and apparently in place.

646 Report oF THE STATE GEOLOGIST.

The dip is 6°, 8. 50° W. Mr. Darton, in giving a description of the various
layers shown in this quarry assigned to them a total thickness of only thirty-
four and one half feet which is clearly an underestimate.* The greater part
of the wall of the quarry is perpendicular so that there is no difficulty in

measuring it accurately.

South Side of the Mohawk.

On the southern side of the Mohawk river, about two miles east of Fort
Hunter, are clear exposures of the fucoidal beds of the Calciferous, along the
West Shore railroad and in the side of the hill south of the highway.
Quarries in this division of the Calciferous are at present worked by the
Wemple Brothers. A section in the western part of the quarry is as follows:

ALIV ('.. Fine-grained, non-fucoidal layer. =... 930% eee

(”. Fine grained, dark drab, non-fucoidal layer. Main quarry bed. Fe,

C®. Layer merging into the one above, but with tendency to * ip»
divide into thin layers.

C*. Mainly in one thick, compact layer, the upper .part quar- % °_"%°
ried, still greater tendency to split along the middle. Steel-grey color weath-
ering to a mottled light grey and buff.

C®. Three dark grey layers, eight, nine and ten inches below % }_ i} }-
the top.

CG’. Layer not’so fucoidal- as those abével) 0 2h ee

C". Buff weathered layers with pitted surface; the fucoidal ¥f i et
material conspicuous and in horizontal layers.

About 700 feet east of the quarries, Utica slate is exposed in the bed
of a small brook to the railroad level; and about 100 feet east of the
quarries the shale may be seen in the lillside not far above the railroad, the
layers being highly inclined to the east. In the railroad cut not far west of
this point, the fucoidal rock is shown and a section is as follows :

XLIV M™,. Heavy bed with disseminated fucoidal material sf*%,,
separated from layer above by a band of very fucoidal character.

D*. Layer with several prominent buff bands; one very con- ,*°%,
spicuous about four inches wide.

/*. Similar to the following (D*) but with greater number of 5,f°%,
streaks.

/*, Massive bed of even weathering limestone with some obscure g"°%,,

yellowish streaks when weathered.

*Thirteenth Annual Report of the State Geologist [New York], p. 421,

‘Ss ISO 1¥ ‘WMVHO/) SHL SO MNVE HLYON SHL NO SNOLSGNVS SNOYASIONIVD 4O SEE}

WX 3iWid

ProssER AND CumiIncs—Lower SruriAN SEcTIONS. 647

The Calciferous sandrock outcrops frequently along the railroad between
the cut and Fort Hunter. On the side of the hill not far west of the Wemple
quarries, the Trenton crops out and was extensively quarried when the Erie
canal was built.”"* The opening is an extensive one, the wall eight or nine
feet high, but it has not been worked in a long time and is not a favorable

place for collecting.

Ture AmsreRDAM—HorrmMan' Rxecron.

The following sections on the north and south sides of the Mohawk
river, between Amsterdam and Hoffman, will give a clear idea of the litho-
logic characters and thickness of the Calciferous, Trenton and Utica forma-
tions in the eastern part of Montgomery county. The section on the
southern side of the river, to the south of Amsterdam, is especially important
in giving the great thickness of the Utica slate in this part of the Mohawk
valley.

Section along Morphy Creek to the Top of Adebahr Hill.

On the south side of the Mohawk, half way between Crane’s Village and
Amsterdam (Port Jackson), on the estate of Mr. Benjamin Morphy, is an old
quarry in the bed of a creek, which empties into the canal, and which may be
called Morphy creek. One and three-tenths miles south of this quarry, a
north and south line through the latter point passes near the next creek east
of Morphy creek at some distance above its mouth. This line also passes
through Adebahr hill. <A section was measured beginning at the canal level
below the Morphy quarry and extending nearly due south to the top of
Adebahr hill. (Section XLVI F.)

#". Canal level. Thick bedded layers of steel-grey, arenaceous 3f°'x,
limestone with thinner, mottled layers near the top which contain Ophileta
in abundance.

Fr? Medium. dark, dove colored, very compact, fine-grained lime- 4*°°%.
stone, with conchoidal fracture, containing occasional examples of P/ytopsis
tubulosa; weathers light bluish grey. Birdseye limestone.

F. Dark blue, fine grained limestone, somewhat lumpy, weathering '"?°
to an ash-grey. Contains corals. Base of Black river limestone.

F*, Dark blue, fine grained limestone with occasional crystals of ™ 3°

calcite; contains corals and Leafinesguina alternata (Con.), H. and C.

* This quarry is that mentioned by Vanuxem as the Sage and Reed quarry, opposite Tribes Hill (Geology of New York,
Part III, p 37)

648 Report oF THE State GEOLOGIST.

I. Dark blue, fine grained, compact limestone with small sparked 7}
ling crystals of calcite. Fossiliferous.

I. Two feet covered, then one foot of dark blue, fine grained Feet
limestone with sparkling crystals of calcite. Fossiliferous.

#, Somewhat crystalline, blue fossiliferous layer. Base of Mss
Trenton limestone.

F*. Compact, fine grained, bluish-grey layer with glittering #*4,
surface on fresh fracture. Fairly abundant Trenton fossils.

#. Bluish-black, fine grained massive layer, weathering bluish- "Pi? _ i
grey with yellowish fucoid-lhke markings on vertical and horizontal faces.
Well preserved specimens of 2ufinesquina alternata are fairly abundant.

f’®, Uneven, dark, compact, fossiliferous layer with crystalline "2,
lenticles; the fossils mostly in the lenticles.

F™. Dark blue, fine grained layer with crystalline fossiliferous #t2_¥
lenticles which, by weathering darker and yellowish, give a mottled appearance
to the surface.

Fr®. Greyish-blue, crystalline, fossiliferous layer . . . . . . =9™

#*, Dark blue, fine grained, with crystallie lenticles, and 4° "}_%*
weathering similar to No, 11. Fossiliferous.

FF. Medium light colored, weathering with yellowish streaks as f°,
in No. 11. Abounds in Trenton fossils.

#®, Thin, irregular, dark blue, fine grained layers with inter- 7%
calated black, carbonaceous shale. Contains great numbers of fossils,
especially Monticulipora (Prasopora) lycoperdon (Say), and Trinucleus con-
centricus (Eaton), Hall.

i. Utica slate exposed in creek bed and in contact with the f° %-
Trenton below. Thin, even layers of black, carbonaceous, calcareous shale ;
above this, covered to first creek east of Morphy creek. Difference in altitude
between these two points, 270 feet. Utica slate.

FF. Jn the first creek east of Morphy creek, at a point one and 59"©%o
four-tenths miles almost due south of the Morphy quarry, are exposed even
layers of very black, strongly calcareous, slaty shale containing seams filled
with calcite. These thin layers are occasionally interrupted by thicker, com-
pact, very fine-grained layers with conchoidal fracture. The latter resemble
the hard, fine-grained layers of the upper Trenton in No. 15. The dip 1s
uniformly southerly.

Ff, -Oovereds Yo vic Dee eee ee

ProsseErR AND Cumines——Lowerr SriuuriaANn Sections. 649

fr, Black, carbonaceous, slabby, calcareous shale, exposed in the go"

creek bed and to the first branch of the creek, not far below the highway
north of Adebahr hill.

£™. No rock is exposed in place, but plenty of fragments of jF°°ts
calcareous shale occur in the soil of the hillside, becoming especially abundant
in a small knoll on the northeastern declivity.

#4. Top of Adebahr hill. Black, crumbling, calcareous shale jy Pa
with thicker coherent layers exposed in the open pasture on the southern
brow of the hill. Below this point covered. The top of Adebahr hill is
barometrically 820 feet above the base of the section. The New York
Triangulation bench mark, seen on its northern crest, is 1,062 feet A. T.
The difference between this and the altitude of the canal at the base of the
section is 800 feet.

The members of the Trenton and Calciferous formations of this section
were measured by Mr. Darton in the summer of 1892, and described in
1894.* In his section the Birdseye is given as above the Black river. There
does seem to be a peculiar blending of the lithologic characters of the mas-
sive member of the Trenton and the Black river in Nos. 8 and 9 of the
present section, so that there is not a sharp line between the two subfor-
mations. The Birdseye is well defined, however, in its proper stratigraphic
position, being sharply separated from the underlying Calciferous, and less
sharply, though distinctly, from the overlying Black river. It contains no,
or at least very few, fossils. The upper, thin-bedded member of the Trenton
is excellently shown and seems to pass gradually into the Utica slate above,
although the line between the two is fairly distinct if drawn where the
Trenton fossils cease. The Utica slate is exposed at intervals from Morphy’s
to the top of Adebahr hill, a vertical distance of 740 feet, with quite con-
stant characters, especially the persistence of slabby, calcareous layers. The
distance between Morphy’s quarry and the bench mark on Adebahr hill is
just three miles, hence if the south dip be 140 feet per mile, the actual

thickness of Utica in this section is 1,160 feet.

Minaville Section.

In the slope of the hill, southwest of Minaville, and at a point about one
and four-tenths miles south by southwest of the centre of the village, the

Utica slate is exposed in several small glens. A section was measured be-

ginning at the level of Chuctenunda creek and extending to the top of the hill.

*Thirteenth Annual Report of the State Geologist [New York], pp. 426, 427.

650 Report oF THE STATE GEOLOGIST.

NLV K'. ,Mostly covered, but showing brownish weathering, 43's;
slabby shale in the west bank of Chuctenunda creek, just above Minaville.
Utica slate.

kK. Top consisting of slaty layers, containing graptolites in "4,
abundance. Below this point the black calcareous shales are exposed to within
165 feet of creek level.

Kk. Black shales, becoming olive to blackish at top. These °°.)
shales show a transition from the black, calcareous, slabby shale of the Utica
to the arenaceous, thin, crumbling, olive shale of the Hudson river for-
mation. ‘Transitional shales.

‘*. Mostly thin sandstones and arenaceous shales, with a massive 447°"; 4)
two-foot layer at the base in the south branch of the deep glen, This portion
of the section comprises the cap of the hill and is mostly covered. Hudson
river formation.

The above section is the only one noticed in this region, which gives the
passage from the Utica to the Hudson river formation, and is of especial
interest on that account. Within the limits of a continuous exposure of 255
feet of shales, there is exhibited a complete transition from the typical
lithologic characters of the Utica to those of the Hudson river. The Utica,
at the lower part of this exposure, is black with brownish streak, and
weathers brown with a greenish tint. It is strongly calcareous and disposed
in even, well defined layers, which usually spht into laminae, having smooth
flat surfaces. These, in turn, crumble to square-edged fragments. In some
cases, however, coherent layers occur from an inch to four or five inches in
thickness, which are quite hard and break with a conchoidal fracture. These
are the well-known slabby layers of the Utica formation. The shale shown
in the upper part of this exposure is blackish to dark olive or grey, very
friable, and weathers to a dirty brown. It is not sufficiently calcareous to
effervesce with cold acid, and is disposed in layers which break up into
regular laminae with uneven rounded surfaces which, in turn, weather to
small, thin, sharp-edged, usually quadrilateral scales that readily pass into soil.
The Graptolite bed is of especial interest and no other fossils were found in
it. The shales at this point exhibit a combination of the characters of the
Utica and Hudson river formations, and the layers split into laminae with
regular surfaces. The difference in altitude between the first exposure of
sandstone in this section and the level of the Mohawk at its nearest point,
is 740 feet, and the distance is nearly five miles. This indicates a thickness

of approximately 1,440 feet, if the dip be 140 feet per mile, as is shown to

ProssER AND Cuminecs—Lower SmurtAn SEcTIONS. 651

be the case later in this paper, at Crane’s Village and Hoffman. As the
thickness of the Utica obtained in this section is much greater than any
previous estimate, it is interesting to review the former statements in regard
to its thickness.

Emmons stated that the Utica slate “in the gorges of Lorrain and Rod-
man is about seventy-five feet thick; it is, at least, less than one hundred
feet ;”' a statement which was repeated four years later in the Agriculture of
New York.? Vanuxem estimated that the maximum thickness of this for-
mation “is about 250 feet,”*? while Dana gave the thickness of the Utica
formation as 250 feet in Montgomery county. More recent estimates are those
of Messrs. C. D. Walcott and C. §. Prosser, derived mainly from well
records. Walcott gave the thickness of Utica slate passed through in the
Campbell well near Utica, as 710 feet; and in a diagram® indicates that the
formation thickens eastward. In the section described by Mr. Walcott along
the south branch of Sandy creek in Jefferson county, he gave 180 feet of
Utica slate with 100 feet of transitional beds above, composed of “alternating
banks of shale and grey, fine grained, calcareous sandstone ; the shales pre-
dominating.”* Prosser gave the thickness of the Utica slate in the
Chittenango well, thirty-two miles west of Utica, as 233 feet, below which are
sixty feet of transitional shale and limestone to the massive Trenton limestone.
In this well 640 feet of blue argillaceous shale and bluish-grey arenaceous
shale and sandstone are referred to the Hudson river. In the Rochester well
the thickness of Hudson river and Utica taken together, is given as 598 feet.
In the Altamont well, about seventeen miles west of Albany, the drill started
595 feet below the base of the Helderberg limestone, which caps the Hudson
river formation in that vicinity, and passed through 2,880 feet of sandstone
and shales before reaching the Trenton limestone.” The thickness of Utica
slate was not ascertained in this boring, but a thickness of 3,475 feet of both
formations indicates a considerable thickness of Utica. Mr. Henry M. Ami
says: “By some of the early writers it | Utica formation] was spoken of as
consisting of shaly strata whose total thickness exceeded 900 feet, whilst by

others the very humble, yet perhaps truer estimate was given of about

1Geology of New York, Part II, 1842, p. 118.

2 Loc. cit., p. 124

3 Geology of New York, Part IIT, 1842, p. 56.

4Manual of Geology, Fourth Edition, p. 494.

5Proceedings American Association Advancement of Science, Vol. XXXVI, p. 212%. Also, Bulletin Geological Society of
America, Vol. I, 1890, p. 347.

6 Tbid., p. 358 (diagram).

7 [bid.. p.348, and see diagram on p. 350.

8 Tbid., Vol. IV, p. 99.

9 Proceedings of Rochester Academy of Science, Vol. II, p. 92.

10 Ashburner, ‘Transactions American Institute of Mining Engineers, Vol. XVI, pp. 951, 952.

652 Report OF THE STATE GEOLOGIST.

seventy-five feet in thickness.”* .The highest estimate for Montgomery county
is that of Vanuxem, also taken by Dana, of 250 feet. Mr. Walcott’s diagram,
already alluded to, would indicate a thickness of 800 or more feet in this
region, but 1s not a formal estimate. Two hundred and fifty feet is the
generally received estimate of the thickness of the Utica slate in Montgomery

county.
The Eva’s Kill Section.

Along the Eva’s lull, which empties into the Mohawk river, just west of
the Crane’s Village station, are numerous exposures of Calciferous sandrock,
and about one and one-half miles back of Crane’s Village is a small isolated
hill just west of the highway, capped by the lower members of the Trenton
formation. The section beginning at the level of the Mohawk and extending
to the top of the hill is as follows:

XLV <A}. Mostly covered. Top consists of massive, thick- Ff
bedded, grey, calcareous sandstone exposed in the bed of the Eva’s kill.
Ninety feet from river level to base of exposure.

A’, Partly covered. Heavy bedded, compact, calcareous sand- °@*hs
stone.

A®, Medium to thin bedded arenaceous limestone with fucoidal 3f° 4.)
markings, especially near the top where the color is dark blue and the
weathering very light ash-grey. Contains iron pyrites. From level of Eva’s
kill to the Manny corners highway, 130 feet.

A‘. Mostly covered. Calcareous sandrock exposed at the base j°%o9
in the road above the Eva’s kill and at the top in the side of Quarry hill,
where it is thin bedded and mottled, and weathers with rough, jagged surface.
Top of Calciferous sandrock.

A°. Dove-colored, with flat conchoidal fracture; disposed in 4F*.
thin layers, weathering more unevenly than usual for this hmestone. Birdseye.

A®. Dark blue-black, fine grained, lumpy, heavy bedded lime- , Fi,
stone, containing Coluimnaria alveolata. This fossil ranges through eight and
one-half feet of compact lmestone and marks an horizon which varies in
thickness from seven to nine feet within the limits of the quarry.

A‘, Greyish-blue, semi-crystalline limestone, weathering dark f°,
ervey, containing several small specimens of Codwmnaria and abundant crinoid
segments. In places the rock is filled with pebbles of sandrock, which are

similar to the Calciferous.

* Reprint from Canadian Record of Science, October, 1892, p 3.

Prosser AND Cumtincs—-LowrErR SILuRIAN SECTIONS. | 653

A’. Thin bedded, dark blue limestone; abounding in fossils, ,"°%is
including Lafinesquina alternata (Con.), Hall and Clarke.

This section presents several interesting features. The upper part of
No. 3, representing the Fucoidal member of the Calciferous formation, is of
unusually dark color and weathers almost as light as the Birdseye. The
surfaces of the layers are often covered with the markings which have
suggested the name by which this rock is known. In the side of Quarry hill,
the Calciferous sandrock seems to present a somewhat transitional character,
becoming less and less arenaceous toward the top. Capping these layers in the
eastern brow of the hill are the two and one-half feet of Birdseye mentioned
in the section; but Just over the brow of the hill in the northeastera part of
the quarry the fossiliferous Black river beds are seen to rest directly on grey,
arenaceous rock. Apparently the Birdseye has totally disappeared within a
distance of two rods. In the western part of the quarry there is again a dove-
colored, fine grained limestone below the Co/uwmnaria horizon. In the central
part of the quarry the Co/umnaria ranges through from seven to nine feet of
very compact limestone. In this part of the quarry also occur the pebbles of
Calciferous (?) imbedded in a layer which caps the massive Black river bed.
This layer also contains several small specimens of Co/umnaria, but the latter
may have been derived in the same manner as the pebbles, from fragments of
lower strata. In the south side of the quarry the layers corresponding in
position to the Black river contain an abundance of iron pyrites and pockets
lined with crystals of white calcite. At this point the upper surface of the

rock is striated, the striae running N. 85° W. The dip is in general about
24°. S.20° W. Vanuxem has noted the presence of pebbles about Amsterdam
similar to those mentioned above. Speaking of the base of the Trenton, he
says: “One of the lower layers at Putnam’s quarry [Tribes Hill] shows some
scattered irregular pebbles, forming masses or concretions having the same
character in all respects as the yellow-colored Calciferous sandrock, and
accurately resembling those observed in a quarry at Shelpintown | Rockton |;

the largest of them are fully four inches in diameter and of greater length.” *

Section opposite Crane’s Village on the south side of the Mohawk River.
Opposite Crane’s Village} station, the cut on the West Shore railroad has
exposed the Calciferous sandrock, and a section, beginning at this point, is as

follows:

* Geology of New York, Part III, 1842, p 44.
t This place is given as Cranesville on the Amsterdam sheet of the United States Geological Survey ; but is known locally as
Crane’s Village and is so given on the timetables of the New York Central aad Hudson River railroad

654 Reporr oF THE STATE GEOLOGIST.

XLVI C’. Medium to thin bedded calcareous sandstone. Layers 5."°%

2 — 52
irregular. To canal level. Calciferous sandrock.

C*. Heavy bedded, massive arenaceous limestone. . . . . . 9%
C®, Mostly covered. Steel grey arenaceous limestone, containing "°"5;

flint and calcite.

C*, Dove-colored, very compact, even bedded limestone with flat 2, _ &%
conchoidal fracture, and weathering ash white. This rock contains abundant
examples of Phytopsis tubulosa and rests upon buff arenaceous limestone.
Birdseye limestone.

C°®. In the large quarry, just east of the small creek that empties ,"°%;
into the canal, a few rods east of the cut, is exposed dark bluish-black, mas-
sive, fine grained limestone, which weathers light and contains Black river
corals. Black river limestone.

C®, About 200 yards east of the creek is a large quarry in which 4°44
the basal layers are thick, even bedded and somewhat crystalline, and weather
light bluish-grey. They contain Pafinesquina alternata and other Trenton
fossils. Base of Trenton.

C". Above the heavy layers of C* are thin, irregular, dark blue ,.¥°4,
layers abounding in fossils.

C®. Base of Utica. In the bed of the creek, near the highway, :4°"ha,
black, even bedded, calcareous shale. The difference in altitude between this
point and the top of the hill, just to the south, is 148 feet. Utica slate.

At the railroad cut, where Nos. 1 and 2 of the above section are exposed,
the rocks of No. 1 exhibit a rather abrupt bending of the layers. Near the
eastern end of the cut is a nearly vertical line, east of which the dip is ten
degrees east, and west of which the dip is one degree west, or nearly normal.
This section furnishes the best outcrop of the Birdseye limestone to be found
anywhere in this region. At this place the Birdseye presents the characters
so typical of it along the northern branches of the Mohawk river to the north-
west. It is dove-colored, impalpably fine grained, with flat conchoidal fracture,
smooth vertical joint faces; and weathers ash white with a delicate bluish
tint. The peculiar plant-like reticulations of Pihytopsis tubulosa are very
conspicuous in the rock at this locality, since they weather buff, whereas the
rock matrix weathers nearly white. The vertical columns, the extremities of
which give the “ birdseye” appearance to the surfaces of the layers, are larger
than in the rock of this subformation near Newport and Little Falls, where
they are quite small and composed of calcite, while in the Birdseye of the

lower Mohawk they are composed of argillaceous material. Within the ~

to}

Prossrr AND Cuminecs—LoweEr SrurtaAn SECTIONS. - 655

himits of the exposure—a small quarry—this limestone varies from two to
four feet in thickness, both delimiting terranes being in place. The upper
surface of the subjacent Calciferous sandrock is irregular, and the line of
contact between it and the overlying Birdseye very sharply defined. Above,
the Birdseye seems to pass into the superjacent Black river limestone without
any sharp line of demarkation.

The base of the Trenton formation in this section is approximately 880
feet A. T., while in the exposure west of the Eva’s kill, one and one-half miles
north, the base of this formation is 600 feet A. T. This gives a south dip of

147 feet per mile.

Hoffman and Van Epps Hill Section.

Just west of the railroad station, at Hoffman, Schenectady county, is a
conspicuous cut on the New York Central railroad, in which the Calciterous
sandrock is well exposed. The base of the cut is about twenty feet above the
Mohawk river. <A section, beginning at river level and extending to the top
of Van Epps hill, is as follows: }

IT A’. Massive, thick-bedded, steel grey, arenaceous, buff- ag?%o9
weathering limestone or calcareous sandstone ; the lower twenty feet covered
beneath the railroad, and forty-eight feet immediately succeeding, exposed
in the cut. Above the cut, partly covered. The joints and seams of this
rock are often filled with calcite, and some chert occurs.

A*, ‘Top covered for the most part; base consisting of dark blue, 4o"2%Iso
moderately fine-grained, arenaceous limestone, with weathered surface marked
by plant-like reticulations which weather yellowish, exposed in the roadside at
an elevation of 350 feet above river level. Fucoidal division of the Calciferous.

A®. West of the Schenectady-Montgomery county-line road, at ;"°%.
an altitude of 850 feet above river level, is a five-foot bed of compact lime-
stone, containing a large specimen of Columnaria alveolata near the base.
Black river limestone.

A*, In the fault escarpment, a short distance to the northeast of 5.f°%S.,
the exposure of No. 3, is another of about twenty-five feet of thin, hard,
‘dark-colored layers, containing Trenton fossils including Zrinucleus concen-
tricus. These layers rest directly upon thick layers of Calciferous sandrock,
and from this fact and their strong dip, it is probable that they were displaced
from their normal stratigraphic position in the faulting. In the open field
east of the highway, opposite the exposure of Black river, and at an altitude

of about 850 to 355 feet, is a small exposure consisting, at the top, of three

656 Report oF THE SvTatTeE GEOLOGIST.

feet and eleven inches of grey crystalline limestone (Trenton). underlaid by
two and one-half inches of limestone weathering ash white (Black river ?),
then seven inches of crystalline rock (Trenton), and finally, at the base, three
and one-half feet of compact light-weathering limestone. In the field on the
west side of the road and opposite a farm house, a short distance beyond the
exposures of No. 3, are exposed at the top eight inches, in two thin layers, of
rather coarse grained, semi-crystalline limestone, containing fragments of
brachiopods, trilobites and crinoids. Below this is one foot, in thin layers, of
fine grained, drab-grey limestone, weathering ash white and apparently barren
of fossils. The basal layer is bluish-drab to grey, coarser grained, and has a
thickness of four inches. Five feet above the top of this exposure, and a
short distance east of it are five feet of crystalline highly fossiliferous lime-
stone. These five feet of rock should be added to the twenty-five feet seen in
the fault line, as it is a representative of layers not shown in the latter place.
Trenton, with possibly Black river at base.

A®, Black, caleareous shale seen mainly as small brown-weathered ,,("°t,,
fragments in the side of Van Epps hill; in only a few places is evidence of
stratification preserved. Utica slate.

This section has been carefully studied by field parties from Union
College, and the measurements above given have been compared with those
obtained on several such excursions, so that they may be considered to possess
a fair degree of accuracy. This section, it will be noticed, gives 350 feet of
Calciferous sandrock measured in an almost vertical ascent. As the gneiss is
not brought up here, the total thickness of Calciferous is not shown; but
enough is shown to indicate that in this eastern region the Calciferous sand-
rock is a thick formation though, perhaps, not attaining as great a thickness
as at Sprakers and Little Falls.

The Pattersonville Section.

About one mile west of the Pattersonville station, on the West Shore
railroad, is a long cut made partly by the excavation for the canal and partly
by the West Shore railroad. A section was measured at this locality begin-
ning at the bottom of the canal.

IT BL. Bottom of canal. Compact thick bedded, steel-grey, 4g°°*%,
arenaceous limestone weathering yellowish and containing abundance of flint
and calcite. The dip at the western end of the railroad cut is about 4°,
N. 55° W., and at the eastern end 4° in the opposite direction. Calciferous
sandrock, thirty feet in the canal cut and eighteen feet in the railroad cut.

Prosser AND Cumincs—-LowER SILURIAN SECTIONS. 657

L°. Above the cut and through the fields to an old quarry, are jy",
numerous exposures of massive arenaceous limestone having, especially in the
lower layers, fucoidal markings. Fucoidal member of the Calciferous.

L°. About one-half mile southwest of Pattersonville, and at the ,*t,
head of a small run, is a small quarry to the south of an old limekiln. The
Calciferous is exposed in thin layers at the bottom of the quarry in the run,
and resting upon it is a layer about a foot in thickness, of bluish-drab fine
grained limestone which weathers ash grey. The outlines of several fossils
are shown on the surface of this layer, and notably that of the cephalic shield
of a large trilobite (Asaphus platycephalus?). Above this are exposed about
five feet of thin, bluish-black, fine grained, irregular, lumpy layers, weathering
light ash-grey and abounding in fine specimens of Columnaria alveolata,
Goldfuss. In the east side of the quarry the rock is exposed in thicker
layers, the lower containing Columnaria. Just over the fence to the
east is a larger quarry in which the upper layers of the former quarry are
exposed and contain large masses of Columnaria alveolata in the same strati-
graphic position. In this quarry the light-weathering layers are capped by
dark-weathering, crystalline layers. Black river limestone.

S*. A short distance south of the exposures of No. 3 is an ,*e%t,
extensive quarry, the western end of which is known as the Walker quarry,
and the eastern end as the Moore quarry.* ‘The lowest rock exposed in these
quarries is dark, bluish-grey, crystalline limestone, massive and weathers
bluish-grey. Highly fossiliferous. Heavy bedded member of the Trenton.

°. Resting on the massive layers are thin, irregular dark blue layers
of fine-grained limestone with intercalated black carbonaceous shale. Highly
fossiliferous ; especially rich in brachiopoda.

B®. Covered from top of limestone in the quarry to lowest ft,
exposure of shale in an open drain south of the quarry.

B’. Black, argillaceous shale to the top of the hill. Utica slate. ,,7¢t..

The above section is of interest on account of the excellent exposure of
the fossiliferous Trenton and Black river limestones, and from the fact that
it affords an opportunity for determining the south dip by comparison with
the exposures across the river exactly one mile to the north. The base of the
Trenton limestone on the north side of the river is approximately 590 feet

A. T., and on the south side 450 feet, giving a southerly dip of 140 feet

co)

per mile.

* Bulletin New York State Museum, No. 3, 1888, p. 105.

+2

658 Reporr oF THE STATE GEOLOGIST.

The thin-bedded limestones of B? are very fossiliferous, this quarry being
one of the best localities for the collecting of Trenton fossils in the lower

Mohawk valley. From A‘ and A® the following species were collected :

1. Monticulipora (Prasopora) lycoperdon, (Say). (a)
2. Stictopora elegantula, Hall. (c)
3. Rafinesquina alternata (Con.), Hall and Clarke. — (aa)
4. Plectambonites sericea (Sowhb.), H. and C. (c)
5. Orthis (Dalmanella) testudinaria, Dal. (c)
6. Orthis (Dinorthis) pectinella (Kmm.), Hall. (7)
7. Phynchotrema capax (Con.), Hall. (1)
8. Raphistoma lenticulare, Emm. (2) (1)
9. Murchisonia bellicincta, Hall. 3)
10. Murchisonia gracilis, Hall. (1)
11. Asaphus platycephalus, Stokes. : (c)
12. Trinucleus concentricus, Eaton. . (1)
13. Dalmanites callicephalus (Wall). (1)
14. Leperditia fabulites (Con.). (c)
15. Schizocrinus nodosus, Hall. (a)

Segments of stems.

To the southeast of Pattersonville, and west of Rotterdam, is the high
and steep hill named Waterstreet on the Amsterdam topographic sheet of the
United States Geological Survey. The top of the northern end of the hill is
given as 1,385 feet A. T., and the rocks from near the level of the Mohawk
river to the top of the hill consist of alternating layers of shales and sand-.
stones which belong in the Hudson river formation and give a thickness of
some 1,125 feet. This, of course forms only a part of the thickness of the
Hudson river formation, since it was shown by Ashburner that at Altamont,
some ten miles to the south, the thickness of the Hudson river and Utica for-
mations taken together is 3,475 feet.*

Nine-tenths of a mile west of the Schenectady pump station, on the West
Shore railroad, are a deep glen and a long cut. The section of the glen and
cut is as follows:

I 0. Covered from level of Mohawk river to Erie canal... . . . f@t.

(*, Fine shale which at the base of the glen does not weather ,,(°°°%s,

readily to soil. Graptolites are fairly abundant.

C®, ‘Very fragile shale exposed in the railroad cut. . . . 3. yeaa;
C* Thin sandstone layer: ><. 0520 ieee eee

* Transactions American Institute of Mining Engineers, Vo}. XVI, pp. 951, 952.

ProssER AND Cumincs—LOoOWER SILURIAN SECTIONS. 659

em eh CREE Lah ratte Bre 5) a wifm a 7 HE Ngee ey, dao! ogg hee

lia 7 148y5
C®, Thin layer of sandstone.
Ce crim mnevarenaceous shale..." 2 se fete me wv ght

C8’. Heavy layer of sandstone by the highway which runs under ,Fe¢t
the railroad track east of the cut. Dip, 3°, 8. 50° W.

From a very thin layer of loose grained, arenaceous shale exposed near
the base of the railroad cut on both sides of the track and largely composed
of the comminuted fragments of fossils, the following species were collected:

1. Triarthrus Becki, Green. (c)

Numerous small fragments of the pleurae and a few complete
specimens of the glabella.

2. Trinucleus concentricus, Katon. (c)
Mostly fragments of the spines and cheeks.
3 Plectambonites sericea (Sowb.), H. and C. (?) (c)
All the specimens are very small and rather coarsely striated.
4. Orthis (Dalmanella) testudinaria, Dal. (2) (r)
5. Orbiculoidea sp.
6. Monticulipora (Prasopora) lycoperdon, Say (2). (r)
7. Crinoid segments. (r)
8. Graptolites.

GEOLOGICAL SURVEY OF THE STATE OF NEW YORK.

(GEOLOGICAL MAP.)

REPORT
ONSTHE TAL€ INDUSTRY OF ST. LAWRENCE. COUNTY.

JAMES HALL, | CoE SEY RE: Jin.
State Geologist. | Assistant.

1895:

661

James Han, State Geologist,

Sir:

The accompanying report on the tale industry of St. Lawrence

county embraces certain results of my investigations in this region which it

has seemed well to bring together in a special chapter.
Respectfully yours,

Cera SiEY TECe Ir:

Hamitton Couiecr, Cuinton, N. Y., Lebruary 27, 1896.
663

Report on the Talc Industry of St. Lawrence County.

By C. H. Smyrn, Jr.

* an account was given of the southwestern portion

In a former report,
of the tale deposits, which extend from the central part of the township of
Fowler, nearly across Edwards. The examination then made was incidental
to a reconnaissance of a portion of St. Lawrence county not including the
town of Edwards in which the tale has its greatest development. On this
account, the description of the deposits was very incomplete, and the con-
clusions drawn as to their origin were limited to such portions as were
actually studied. The explanation of the deposits suggested was, however, of
such a nature that it was difficult to see how it could apply to a part of
them and not to the whole; and this general application was withheld simply
because the descriptions of the tale in Edwards, which had been published at
that time, were so at variance with the facts observed in Fowler. In the
latter town, as stated in the report referred to, the tale gives every indication
of being a bedded deposit, constituting a portion of the crystalline limestone
formation so important in this region.

Published accounts of the tale in Edwards, however, stated that it formed
a clearly-defined vein, with granite or gneiss walls.+ As it hardly seemed
possible that the tale should exhibit such different relations at poimts on a
continuous belt and separated by only a few miles, it was thought advisable
to examine the entire series of deposits, their economic importance being
sufficient to warrant a determination of their geologic character.

Such an examination, made during the past summer, served to remove
the seeming contradictions which formerly existed. The deposits in Edwards
were found to agree in every important particular with those of Fowler, and
all the facts observed are in harmony with the explanation given for the
latter. The deposits only remotely resemble veins, while the walls of granite
and gneiss have no existence.

The chief mines form a group in and near Taleville, and here the tale is

well shown. It occurs in two or more horizons only a few feet apart, forming

* Report of the New York State Geologist for the year 1893, pp. 493-515.
+ A. Sahlin ; The Talc Industry of the Gouverneur District, St. Lawrence county, N. Y. ; Transactions American Institute of
Mining Engineers, Vol. X XT, p. 583.
Talc ; The Mineral Industry, Vol. I, p. 435.
665

666 Report oF THE STATE GEOLOGIST.

beds from ten to above twenty feet thick, averaging about sixteen feet. The
beds dip to the north and strike northeast, conforming in both respects with
the crystalline limestone in which they he. The walls of the tale consist
of a tremolite or enstatite schist which passes over gradually into the
limestone.

While, in mining, the tale is easily separated from its walls, every possible
gradation exists between the two rocks, and it is evident that they are
different phases of one rock body. The schist probably has resulted from the
metamorphism of a siliceous and magnesian portion of the limestone, being ¢
product of the general metamorphism of the region. Subsequently, parts of
the metamorphic silicates have been altered into tale by addition of water
and loss of lime. This alteration, while most pronounced along certain hori-
zons in the schist, is more or less irregular, causing variations in the thickness
and precise location of the tale beds, which are further increased by
mechanical disturbances.

Most of the Edwards tale shows the fibrous structure of the original
minerals and, in fact, as at the Fowler localities, contains a greater or less
amount of residual tremolite or enstatite. This 1s shown by tests of the hard-
ness of different parts of specimens, or, still better, by a microscopic exami-
nation.

The formation of the tale by the process suggested (and discussed more
at length in the previous report) would not be a merely superficial pheno-
menon, like weathering, but would be the work of solutions which might
extend to great depths, and there seems to be no reason for fearing that the
deposits may be shallow and quickly exhausted. As a matter of fact the
weathered material at, and near the surface, is very poor, good tale appearing
only at some depth where it has been protected from the attack of superficial
agents.

As it comes from the mines, the tale 1s white with a more or less intense
tinge of green. Its lustre is silky or pearly, and its structure decidedly
fibrous. Mingled, however, with the fibrous tale there is often some that is
scaly or wax-like. The latter variety is nearly always developed upon the
surfaces of the rather abundant slickensides.

At the present time ten mines are in operation in the tale district, all but
one, that of the American Company described in the previous report, being
situated at Taleville.

The product of the American Company’s mine is ground by steam power

ia a mill situated only a few rods from the mine, but the other mines send

Smytu—Tarc Inpustry’ or Str. Lawrence County. 667

their product over the recently constructed Gouverneur and Oswegatchie
railroad, to mills scattered along the Oswegatchie river, which furnishes their
motive power.

The process of manufacture is purely mechanical, having for its aim the
reduction of the tale to a fine powder of uniform grain and free from grit.
On account of its fibrous structure, the tale, when powdered, has a strong
tendency to pack into a sort of felt. For this reason it can not be bolted,
and special methods of treatment are required.

The process begins with a sorting of the material at the mines, where the
hard and darker-colored pieces are thrown out. The good tale, in lumps
ranging from a foot or more in diameter down to coarse powder, is then
loaded on cars and shipped to the mills. Here it passes through Blake
crushers, and then goes to rolls or burr stones and is reduced to grains about
the size of a pea.

From the rolls or burr stones, the tale goes either to Griffin mills
or direct to the Alsing cylinders. T hese are drums of half-inch steel, six
feet in diameter and ten feet in length. They are supported by trunnions
at the ends, and revolve about twenty-five times a minute. The cylinders
have a lining of glazed brick, and in each one are placed some three and one-
half tons of round flint pebbles, about the size of an egg. A cylinder is
charged with an amount of tale equal to one-quarter or one-third the weight
of flint pebbles and, after the manhole is closed, is revolved till the tale is
reduced to the requisite degree of fineness. This operation usually takes
about two hours. When it is completed, the closing plate is removed and a
erating substituted, which will retain the pebbles and permit the discharge of
the tale. The cylinder is then revolved again till the tale is all removed,
ready for packing and shipment.

Several grades of tale are produced, varying in fineness and. color.
Extreme and uniform fineness and a blue-white color, are the desirable
qualities. The fibrous structure is found in all grades and is, doubtless, a
most important factor in giving value to the material. The felting of the
powder, which gave much trouble in the earlier attempts at manufacture, is
the foundation of its most extensive application. Under the microscope, even
the finest and most impalpable portions of the powdered tale are seen to con-
sist of ragged, fibrous masses, elongated in the direction of the fibres, and
frayed and shredded at the ends. It is evident that the fibrous structure
is present on so minute a scale as to extend to the finest particles of the

mineral.

668 Report OF THE STATE GEOLOGIST.

This structure alone, howeyer, would not suffice to give to the material
its valuable properties; indeed, it is not an inherent property of tale but,
instead, is a product of its mode of formation. The value of the tale follows
from its complex origin, in virtue of which it combines the fibrous structure
resulting from its derivation from the other silicates with its own pliability
and softness. The value of either mineral in its typical form would be
much less than that of the material which combines some of the properties
ot both.

Tremolite and enstatite, although fibrous, would, on account of their
brittleness, grind to a granular powder with no binding properties; and
the same would be true, though perhaps to a less degree, of massive or
fohated tale.

In the district under consideration the terms “massive” and “foliated ”
are often applied to varieties of tale in which the fibrous structure, although
present, is so fine as to be inconspicuous, except under the microscope. In
such cases, the character of the ground material is the same as of that pro-
duced from the coarsely fibrous talc; although sufficient tale that is truly
massive or foliated may sometimes be present to render the grinding more
difficult and the finished product of less value.

The presence of scales of talc, in many specimens, indicates that it can
not be regarded as entirely pseudomorphous, as these scales certainly do not
have the form of the original minerals. On the contrary, the form is that of
tale itself and must have resulted directly from the independent growth of
that mineral. The materials, doubtless, were supplied by the constituents of
the schist, but the structure of the latter, physical as well as chemical, has
broken down. From this, it seems possible that the fibrous structure of the
deposits may be an indication of a lack of completeness in the process of
alteration which, if continued to its ultimate end, would convert all of the
schist to scaly tale. From what has been said above, it is evident that the
possibility of such a complete change of structure has an economic bearing, as
it would result in the destruction of the most valuable properties of the tale.
From this point of view the question is two-fold, involving the possibility of
such a complete change, and the probability of its taking place at moderate
depths, so as to put a stop to profitable mining. On neither of these points
are there conclusive data at hand but, while it is not impossible that such a
complete alteration may have occurred in some portions of the deposits, it
would, doubtless, be very irregularly distributed; and as it would be inde-

pendent of the present topography, would be developed, at such depths as to

SmytrHo—Tatc Inpustry’ or Str. Lawrence County. — 669

prevent further working, only by a coincidence. For these reasons, it seems
entirely justifiable to neglect this factor in estimating the extent and value of
the deposits.

In the case of most mine products, the chemical composition is the most
important feature, the aim being to secure the greatest amount possible of
one or more constituents of the material mined and in a condition suitable
for extraction. With the talc, this is not so; its value is entirely dependent
upon its physical properties, and its chemical composition is of importance
only as it conditions these. The connection between physical properties and
chemical composition is, of course, most intimate, and hence the composition
is of importance indirectly. The value of the material does not, however,
depend upon the presence of some one element which is to be extracted, but,
instead, upon the character resultmg from the union of all the elements
present.

If any one constituent can be said to have particular value, it is the
water. Its importance les in the probability of its giving the soft and pliable
character to the mineral. Of course, it is Impossible to say that this is posi-
tively the case, but it is a familiar fact that many minerals which contain the
elements of water are softer than other minerals having nearly the same com-
position aside from this constituent. In using the term “water” in this
connection it is not meant to imply anything definite as to the condition in
which its elements are present; for in most cases, as with the talc itself, this
is a disputed point.

The predominant importance of the physical properties of the tale ren-
ders simple mechanical tests of more practical value than elaborate chemical
analyses in determining its grade. Were the material of sufficient value to
demand careful discrimination in dealing with it, microscopic examination of
the powder would perhaps afford the most accurate method of grading. By
this means the perfection of fibrous structure, together with the relative
amounts of talc, tremolite and foreign impurities could be rapidly determined.
With existing prices, however, such refinements are unnecessary.

A chemical analysis, of course, shows whether the alteration of the schist
into tale is complete and, if made on a sample taken from a fibrous mass, is a
thorough test of the value of the material. But aground sample might afford
an excellent analysis, and yet lack entirely the fibrous structure necessary to
give it the desired binding properties. In this way, a purely chemical exam-
ination might lead to very inaccurate conclusions as to the quality of the

material.

670 Report OF THE Stave GEOLOGIST.

The following analyses suffice to indicate the composition of the tale:

ie Il. jE IV. NV;

SiO, Sal lyse anes oO ys) 52.42 61.28 62.10
ALLOn is Soh eer arena eales Rex
Fie,(u Sav es de, ee ot oo. enh ete aes
FeO Oe Qdhar th?) fiiddtinge, Waleed Bie 1.30
MnO 1. 16 0.76 iawn Hee One Das
MgO 34.72 31.37 36.24 26.58 32.40
CaO niice ei; eee Os Dhl eats chctegr Me aes bite ee
Nag) acter eas ae ee OS AB oo An eee dati ee eee eee
H,O Sisthik G22. PC Rae gee 2.05

Getalts Aaa 100.58 99.85 88 .66 87.86 100.00

All of these are analyses of fibrous tale, except III, which is the foliated
variety. I and II are from Dana’s System of Mineralogy, page 679; ILI and
IV from “The Mineral Industry,” Volume I, page 425; and V is communti-
cated by Mr. A. J. McDonald, Superintendent of the International Pulp
Company, to whom the writer is indebted for much information used in the
preparation of this report.

The figures shown in I, II and V agree quite well with the theoretical
composition of tale, and present some features which seem difficult to
reconcile with the hypothesis offered to account for the formation of the
deposits, notably the small amount of lime and alumina. But it is probable
that these analyses are made on selected samples, and that the average com-
position of the product of the mines would show more of these impurities.
Moreover, the thickness of the deposits makes it possible to mine only the
best and most completely altered material, thus tending to keep the average
composition fairly close to the theoretical percentages. That there are, how-
ever, wide variations, is shown by the incomplete analyses, III and IV, which
probably represent the ground product.

During the past year the industry has been in a fairly active state, though
not so flourishing as formerly. ‘The output for the year is estimated, by a
competent authority, to be about forty thousand tons. The selling price of
the finished product ranges from seven to twelve dollars, depending upon the
quality.

The great bulk of the product is used as a filler and weighter in the

manufacture of the medium grades of paper. Its value here is a result of its -

Smyru—Tatc Inpustry or Sr. Lawrence Coun'ry. * 671

fibrous and pliable character, which causes it to be retained in the paper
pulp, to which its binding properties give added toughness. Formerly,
various clays were used as fillers, but these did not strengthen the paper, and
only thirty to forty per cent. of the clay was retained by the pulp, while of
the tale, seventy to nmety per cent. is retained.

Smaller quantities of tale are used in the manufacture of cheap grades of
soap, in toilet powders, in the adulterations of various substances, and in the
manufacture of dynamite.

There seems to be no reason for doubting that the demand for tale will
continue, and increase with the revival of business interests in general. As
existing plants can largely expand their output at any time, it is not probable
that any new properties will be developed in the near future. The many
advantages enjoyed by the plants now in operation are sufficient to prevent
new competitors from entering the field, unless there be some great increase
in the demand for tale. The present conditions are not such as to stimulate
search for new deposits, and past efforts in this direction have not been
encouraging. ‘The great extent of crystalline limestone in the region makes
it probable that other tale deposits exist, but tt would be surprising if any
which equal in size and quality the deposits now worked, should have

remained undiscovered till the present time.

CEOLOGICALD SURVEY OF THE STATE OF NEW YORK.

PHYSICAL TESTS OF THE DEVONIAN SHALES OF NEW YORK
STATE TO DETERMINE THEIR VALUE FOR THE
MANUFACTURE OF CiLAY PRODUCTS.

JAMES HALL, HEINRICH RIES,

State Geologist. | Assistant.

43 amie } “613

Physical Tests of the Devonian Shales of New York State
to Determine their Value for the Manufacture
of Clay Products.

By Heryricnu Ries.

The extensive developments, in recent years, of the manufacture of clay
products having an impervious or vitrified body, as well as strength and
toughness, has led the manufacturers of these goods to experiment consider-
ably in order to determine what class of clays is best suited for the production
of them. The result of these experiments has been the almost universal
adoption of shale for this purpose.

The production of a vitrified body depends on the proper amount of
fusible impurities in the clay, and that these fluxes shall be of such nature
that the clay can be brought to vitrification without danger of its becoming
viscous. It is in shales that these qualifications are usually found.

An extensive branch of the clay-working industry depending upon
shale for its support, has thus sprung up. The product is principally paving
brick and sewer-pipe.

Some idea of the extent to which shale is used may be gained from the
following figures of production given in the “ Mineral Resources” of the
United States Geological Survey, for 1895. The states given are those in

which shale is almost exclusively used.

PRODUCTION OF VITRIFIED PAVING BRICKS IN 1895.

STATE. THOUSANDS. VALUE.
Paina es a gs. } DBOO $23,500
Mencia ete Ne sh ko eels 1s “82,026 643,997
INHALT kek ald DOBLE 204,000
Pee ee Wet ee lon Ey oe FOLIOS 243,928
IN CAS SCOU TEE ae PRS ee 00 A) 54,640
Ivenuork @y, ee oS" Se gl 105896 121,892
OO tie eo sete as) aks ve “OOOO 787,878

Ais alige tte, 2 calles Sie % ber SHG. LO $2,079,835

Report oF THE STATE GEOLOGIST.

for)
SI
(op)

These figures, though large; do not include other shale products, such as
sewel-pipe, stoneware, terra-cotta, pressed brick, ete., and as will be seen from
them, Ohio and Illinois are the largest producers. The works in these two
states have been erected on a large scale, and the products find a wide
application.

Until recently shale was little used by clay workers in the eastern
states, but, having become convinced of its value, they are now taking full
advantage of it.

The whole southern half of New York state is underlaid by a formation
including among its members many extensive shale deposits. These have
been tried with success at several points, and their utilization should expand
rapidly in the near future.

General Properties of Shales.

A shale is practically nothing more than a hardened clay, having been
formed in the same manner, viz.; as a fine sediment deposited in the quiet
portions of lakes or seas, but subsequently hardened by burial under other
sediments laid down upon it.

Although shales are apparently very distinct from clay, on account of
their rock-like condition, the two materials have practically the same physical
and chemical characters, and shale, when ground and mixed with water,
possesses the same plasticity as clay.

Shale-like clay may vary considerably, for just as a clay, by an increase
of its siliceous contents, may pass into sand, so a shale, by an increase of
sand grains in its composition, may grade into a sandstone. This is not at
all an uncommon occurrence.

Shales may also exhibit another change, viz.; passing into slate as a
result of metamorphism. Such slates, when ground and mixed with water,
will never have the same plasticity as shale. They also show a false bedding
developed as a result of pressure, while the original layers of sedimentation
are almost obliterated, the slate showing no tendency to split parallel to them.

At times shales run so low in impurities that they are adapted for the
manufacture of refractory materials. Such shales are restricted almost entirely
to the Carboniferous period (in the eastern United States) and are therefore
not to be sought in New York state.

It sometimes happens that shales are so charged with bituminous matter,
that this impurity has to be taken into consideration in the process of burning,

on account of the enormous heat which it is likely to develop.

Rres—Puysicat Tests or Drvontan SHALES. ~ 677

Most shales contain a large percentage of fusible impurities and it is this
which enables them to burn to a hard, dense, tough body so essential to
vitrified wares, and especially to paving brick. Their action under heat, how-
ever, varies with their physical and chemical properties, which may be briefly
stated.

Chemical Properties of Shales.

Pure clay is fusible only at extremely high temperatures, but the presence
of a shght amount of impurities may lower its melting point considerably.
The impurities found in clays and shales are silica, alumina, iron, lime, mag-
nesia, alkalies, water, organic matter, titanic acid, phosphoric acid, sulphur
and sometimes manganese. Al] these impurities may be placed in one of
two classes, depending on whether they are active or fluxing impurities, or
inert or non-fluxing ones.

Fluxing Impurities.

These, in the order of their effectiveness, are alkalies, lime, magnesia and
iron. The manganese, sulphur and phosphorus would come under this head,
but are seldom present in sufficient quantities fo be worth considering.

“Alkalies. The alkalies in clay may be ammonia, potash, soda and lithia.
The lithia is extremely rare and need not be considered. The ammonia is
frequently present in shales, but as it volatilizes at low temperatures its only
effect is to give a slight, characteristic odor to the material when moist.

Soda and potash are powerful fluxes, which are found in nearly all shales.
They vary in quantity from a trace up to nine or ten percent. This variation
depends on the quantity of feldspar grains present, for this mineral is the
usual source of the alkalies in shales and clays. Aside from the feldspars,
mica may also furnish potash. The mica shows itself as small glistening
scales scattered through the shale.

The alkalies are sometimes present in soluble form as sulphates, which
may cause considerable trouble. In the drying of the clay the water coming
to the surface to evaporate will leave these soluble alkaline salts on the sur-
face as a white coating. In salt-glazing sewer-pipe the sodium vapors from
the salt thrown into the fire unite with the silica and alumina of the clay,
thus forming the glaze. If, now, a coating of these soluble sulphates is pres-
ent, it prevents this chemical union and formation of the glaze. Furthermore,
if the heat is not raised sufticiently to decompose any sulphate salts

678 Report oF THE STATE GEOLOGIST.

present, they may form a white coating on the surface of the burned ware.
The decomposition of sulphates is also accompanied by the disengagement
of sulphuric acid, which, if it escapes with violence, may cause blistering.

Lime is a common detrimental impurity. It is abundant in some mem-
bers of the New York shales, especially those of the Salina group in central
New York. When present to the extent of only two to three per cent. it is
practically harmless. The common source of lime in shales is feldspar, which
is a double silicate of lime and soda; or calcite, which is carbonate of lime.
The latter may be detected by the effervescence produced on the addition of
muriatic acid.

Lime in the condition of silicate may serve as a useful flux, if present to
the extent of four or five per cent.

Carbonate of lime may render a shale very fusible and materially lower
the difference in temperature between the points of incipient fusion and
viscosity. Lime also diminishes the shrinkage of a clay in burning; in fact,
an excess, say twelve to fifteen per cent., may cause the clay to swell slightly.

An excess of lime over iron will counteract the reddening effect of the
latter by the formation of a silicate of lime, iron and alumina.

Seger found that if the lime exceeded the iron in the proportions of three
to one, the product is a good buff. He also found that a good brick could,
with care, be made from a clay containing twenty to twenty-five per cent. of
carbonate of lime, but it is not safe to make a vitrified one from such clay.
Sulphate of ime is not uncommon in some New York shales, and its action
on heating may be the same as described under sulphates of the alkalies.
Some of the marly shales of central New York may be found more suitable
for the manufacture of Portland cement than for clay products.

Magnesia is not an abundant element in most shales, although in some of
the Salina shales it is common. Magnesia is derived from the same classes of
compounds as lime, and, as far as known, exerts the same influence.

Tron. ‘This element acts not only as a flux but also as a powerful color-
ing agent of clay materials, both in their green and burned conditions. It
may exist in clays in a variety of forms, according to the mineral of which it
is a component element. These mineral compounds may be silicates, carbon-
ates, oxides or sulphates. In all these combinations it exists in the condition
of either a ferrous or ferric salt; but in burning, the former generally become
oxidized to the latter, unless the fire is reducing in its action. When pyrite
occurs in the shale, it will, if in grains or lumps, produce fused spots in

burning. It acts as a strong flux.

Rirms—Puysicat Trsts or Devontan SHALES. 679

Ferrous iron compounds are more fusible than ferric ones, and conse-
quently with reducing fire the clay will fuse at a lower temperature; at the
same time, it will not burn to as bright a red. If treated to an oxidizing
fire, the presence of ferrous salts need not be considered. Iron salts are
affected by varying conditions in burning. If the temperature is raised too
rapidly the outer portion of the piece of clay being burned may shrink and
become dense before the air has had time to permeate the clay and oxidize
the iron in the centre of the body. The centre of a brick or other piece of
clay ware may thus be dark and porous while the surface is red and dense.
A further result of this will be a differential shrinkage between centre and
exterior and possible cracking.

Unburned shales may be yellow, blue, brown, red, gray or green in color,
depending generally on the relative amounts of ferrous and ferric salts present.
The same variety of shades and colors is produced in burning. Ferrous iron
alone may impart a green color to burned clay, and ferric oxide red or, with
hard firing, purple. The higher the temperature to which a clay is subjected,

the deeper usually is the color produced by the same amount of iron.

Non-Fluxing Impurities.

These include silica, titanium, organic matter and water.

Silica. This may be present either as quartz combined with alumina
and water in the form of kaolinite, or combined with other elements, as
in feldspar and mica. Silica renders a’ clay more refractory, lessens its
shrinkage in burning and decreases the plasticity. On this account plastic
clay or shale is added to very siliceous ones.

Titanium is a seemingly rare element in clays, due to the fact that it is
seldom looked for in chemical analysis. It is never present in great quanti-
ties, rarely over one per cent., and only exerts a fluxing influence at high
temperatures and when six or seven per cent. of it are present.

Organic matter. Very common in black and in some grey shales, and
may mask the color which any iron present might produce. It may be pres-
ent as finely disseminated particles or in the form of stems or other plant
remains. Organic matter burns off at a bright red heat. Its chief influence
lies in the increased plasticity of a clay or shale, provided an excess of sand
is not present.

Water is present in shales in two forms, viz., chemically combined water
and mechanically combined water or moisture. The moisture in unweathered

shales is generally low, but in mellowed portions of their outcrops it may be

650 Report oF THE Sratre Gronoaist.

.

twenty or thirty per cent. Air drying expels most of the contained moisture
and at the same time a shrinkage of the material takes place. Sandy, coarse
grained clays show the least shrinkage, but fine grained ones may sometimes
show considerable diminution of volume on air drying. The larger the
quantity of water absorbed by a shale in tempering, the more will it shrink
in drying. If the clay is fine grained, rapid drying may cause it to split.
The last traces of moisture are generally driven off in the kiln during the
early stages of burning.

Combined water, This is present in all shales. It usually varies from
three to eight or ten per cent. in shales, depending on the amount of clay
substance and perhaps other hydrated minerals present. Combined water is
driven off at a low red heat, or about 1,200° F., and with the passing off of it
there also begins a second shrinkage. While the amount of combined water
does not stand in any close relation to the plasticity, nevertheless when once

the combined water is driven off, the clay can no longer be rendered plastic.

Physical Properties.

These are considerations of as much importance as the chemical ones, for
they exert fully as much influence on the characters of clay or shale. The
important physical properties which should always be considered, are
fusibility or behavior under heat, plasticity, tensile strength or cohesion and
absorption.

Plasticity. This is one of the two important properties which makes
clay of such use to man, for it permits of molding it into any desired form,
which is retained when the clay is dried. Plasticity, however, is a variable
property, some clays possessing it to only a shght degree, others having
it highly developed. The former are called “lean,” the latter “fat.”
Very fine and very coarse grained clays are generally lean. An excess of sand
also tends to diminish the plasticity, and consequently very siliceous shales,
those passing into shaly sandstones, should be avoided, or should not be used
unless mixed with more plastic material. Organic matter frequently increases
the plasticity of a clay and makes it very fat, unless there is an excess of sand
present. If water be gradually added to dry clay and the mass thoroughly
kneaded, it will be found that its plasticity mereases up to a certain point,
but if more water is added it begins to decrease until finally the clay runs
like soft mud. The amount of water absorbed by shales or clays depends in

general on their plasticity, very “fat” ones requiring the addition of a large

i

Rires—Puysicat Tests or Drvontan SHALES. 68]

quantity of water, and “lean” ones usually needing but little. Of course
there are exceptions to this rule.

The production of maximum plasticity has a practical bearing in the
tempering of the clay, for if too little water is added, the clay will frequently

crack in molding.

Tensile Strength, or Cohesion.

The plasticity of a clay has been found to be due to the interlocking of
its particles,* consequently a mass of clay, when air dried, offers a resistance
(which may be great) to any force tending to pull it apart. This tensile
strength or cohesion stands in close relation to the plasticity, and consequently
serves as a measure of it. The tensile strength is expressed in pounds per
square inch and is determined by forming the wet clay into briquettes of the
same shape and size as those used in testing cement, allowing them to air dry
and then pulling them apart in a cement testing machine.

Jays which appear moderately plastic when worked in the hand, will
show a tensile strength of 100 to 150 pounds per square inch when air dried.
Lean clays may run about fifty pounds per square inch, often lower. Very
plastic clays may show 250 to 300 pounds tensile strength per square inch.

Very fine and very coarse grained shales or clays show a low strength.

Behavior under Increasing Temperature.

Shrinkage. The amount of shrinkage that clay materials undergo in
drying, depends somewhat on the amount of water absorbed or the porosity
of the clay. Coarse grained clays may absorb much water and yet shrink
very little. Having larger pores, they will also permit the water to escape
more rapidly and consequently can be dried quicker, while fine grained ones,
owing to the smaller size of their pores, must dry slowly.

The air shrinkage of a clay begins as soon as it is molded and set out in
the open air or put in tunnels to dry, and continues until all the moisture is
driven off. It may be as low as two per cent. in lean, coarse grained clays, or
reach twelve or thirteen per cent. in others. The highly plastic clays do not
always shrink the most.

The fire shrinkage begins when the combined water commences to pass

off, or at a temperature of about 1,200° F. It may also vary within the same

limits as the air shrinkage. It is, however, affected by several factors. It

* Olchewsky. Tépfer und Ziegler Zeitung, 1882, No. 29.

682 Report oF THE STATE GEOLOGIST.

often increases with the amount of organic matter or combined water present,
and diminishes with the amount of sand which the shale or clay contains.
Lime in excess exerts the same influence as sand.

Between the points at which air shrinkage ceases and fire shrinkage
begins, the clay shrinks little or not at all, therefore in burning clay wares
the heat can be raised rapidly between these two points, but above and below
them it should be raised slowly as long as any water is passing off, to prevent

cracking.
Fusibility.

No clays, on being subjected to a rising temperature, pass suddenly
from a solid to a fluid or viscous condition; on the contrary, they change
slowly from the condition of solidity to that of viscosity. This change may
occur within a range of 75° F., as in very marly shales, while in others it may
require a rise of 400° F. to convert the material from solidity to viscosity.

As the heat is raised to a temperature varying from 1,500 to 2,000° F.
in different shales and clays, the particles of the clay soften somewhat, and
become tightly stuck together. In fact, the individual grains may no longer
remain distinct, and the clay can barely be scratched with a knife. This is
the point of ¢neipient fusion and, as Wheeler* has suggested, this is a good
term to use in defining this stage.

As the temperature is raised from 100° to 200° F. higher (also depending
on the clay), the clay becomes completely vitrified; the body resembles one
solid mass and is impervious or nearly so, The clay has also acquired its
maximum toughness and maximum shrinkage. With an additional varying
rise of temperature, viscosity occurs. ‘The point of vitrification is generally
midway between incipient fusion and viscosity, and these two latter points
may be from 100° to 400° F. apart; the nearer 400° the better. It should
not be less than 200°, otherwise there is the danger of loss in burning, for
with so little margin between vitrification and viscosity it is hard to run the

©

burning to the former point without passing it and reaching the latter.

Manufacture of Paving Brick.

As the most extensive use of shale is for the manufacture of paving
brick, it may not be out of place to describe briefly the methods employed.
Owing to its hard nature, shale generally has to be mined by blasting,

although in some cases, as at Galesburg, Ill, a steam-shovel has been found

* Vitrified Paving Brick, Indianapolis, 1895

Rims—Puysicat Txrsts or Drvontan SHALEs. 683

efficient and economical. The economy of this latter method depends, how-
ever, on its being kept at work as steadily as possible, and consequently it is
chiefly applicable to larger plants.

Preparation. Before being mixed with water or tempered, the shale is
first ground in dry-pans or disintegrators.

Dry-pan. This consists of a circular iron pan with perforated bottom.
In the pan are two mullers about twelve inches wide and supported on a
horizontal axle. The mullers weigh from 2,000 to 4,000 pounds and revolve by
the tangential friction of the pan floor, which is turned by power transmitted
from the engine. Scrapers attached to the axle of the mullers keep the mate-
rial charged, in their path. The shale when ground fine enough falls through
the slits in the pan-bottom. These slits are

generally one-eighth to three-

sixteenths of an inch wide. The capacity of a dry-pan varies with the size
of the screen openings and character of the clay, but one hundred tons in ten
hours with one-eighth inch screen openings is a fair capacity.

Disintegrators, consisting of concentric wheels bearing cross pieces and
revolving in opposite directions, or of an axle bearing steel arms which revolve
between a series of parallel steel bars, are often found effective. The pieces
of shale are ground not only by being hit by the rapidly moving arms, but
also by being thrown against each other.

Screening. The ground shale is generally transported from the dry-pans
or disintegrators to the screens by means of bucket elevators or traveling
belts. Three general types of screen are used.

1. Inclined screens, ten to fourteen feet long, with wire cloth or perforated
metal bottom. They are often provided with a tapping device to keep them
from becoming clogged. Inclined screens are simple and cheap, but have
small capacity.

2. Rotary screens, of cylindrical or octagonal form, usually provided with
automatic devices, such as brushes to keep them clean.

3. Shaking screens, fixed at one end and driven by crank and piston or
eccentric. These are cheap and simple in operation.

While all these screens are designed to perform their work automatically,
still few of them can be left without attention for any length of time.

The tailings from the screens are returned to the crusher or disintegrator.

Tempering is usually done in wet-pans or pug-mills.

Wet-pans. These resemble dry-pans, but have a solid instead of perfo-
rated bottom. The clay is charged in lots of 600 to 1,000 pounds and water
added. Wet-pans are very rapid in their action, a charge for brick or sewer

684 Report oF THE Srare GEOLOGIST.

pipe being tempered in a few minutes. The charge is generally removed by
means of a long-handled shovel pivoted on an upright arm. Wet-pans have a
greater capacity and are more efficient than» pug-mills, but consume more
power.

Pug-mills consist of a horizontal or inclined trough in which there
revolves a shaft bearing knives or a worm screw. The material with water
is charged at one end and, by means of the screw thread or knife blades, is
mixed thoroughly and at the same time passed to the other end of the trough,
where it is discharged. To insure thorough tempering, pug-mills should not
be less than eight or ten feet long. They are extensively used by paving-
brick manufacturers, and so arranged that their contents are discharged

directly into the molding machine.

Molding. Paving brick may be manufactured by one of three processes,

viz., the stiffmud, soft-mud or dry-clay process.

Stiff-mud process. This is the most used by paving-brick manufacturers.
In this process the clay is discharged from the machine through a rectangular
steel die, whose cross-section may be 9x4 or 2x4 inches, depending on whether
the brick is to be end-eut or side-cut. As the bar of clay issues from the
machine it is received on the cutting table and: cut up into bricks, either by a
series of parallel wires fastened to a moveable frame, or by means of a revolvy-
ing wheel, also bearing a series of wires. The capacity of the machine may
be materially increased by having a double or triple die, so that more than
one bar of clay issues at the same time, but a single die will give an
auger machine a capacity of 50,000 brick in ten hours. The clay should
be thoroughly pugged before being charged into the machine. Auger
machines combine economy and large capacity, and their use has not only
become widespread but necessary to enable the manufacturer to compete
successfully with his rivals.

Auger machines are adapted to a wide range of clays, except very lean
or very plastic ones. The former seldom have enough cohesion to hold
together in passing through a die, and the bar of clay cracks and tears. Very
plastic clays develop a series of concentric laminations in the brick which are
a serious detriment to its strength. The laminations in two bricks made from
the same shale may be very differently developed, if molded in machines of
different make. Much attention is, therefore, paid to improving the construc-
tion of the dies and other portions of the machine as small changes may often

cause considerable difference in the structure of the brick.

Rires-—PuysicaL Trests or Drevonran SHALES. 685

Stiffmud brick are frequently repressed, as it is considered to improve
the quality of the product and, indeed, this is true within certain limits.

In a series of experiments recently made by Professor E. Orton, Jr., it
was found that end-cut bricks were tougher than side-cut ones, and when
repressed they were still more so. These experiments are important and
interesting and worth mentioning in detail, A number of bricks were made
from the same lot of shale, but molded on different machines. They were,
however, all burned together in the same kiln. These brick were tested in a
rattler and it was found that the loss by abrasion was least in the case of the
end-cut repressed brick.

Soft-mud process. This method is sometimes used for shales or clays
which can not be molded in stiff-mud machines, and works well. It is being
used at one locality in New York state for the manufacture of paving brick.
The soft-mud process gives a brick of thoroughly uniform texture, but on
account of its limited capacity the cost of production is greater than with
stiff-mud machines.

Drying. Paving brick are generally dried by artificial heat. Two
general systems of drying may be noticed, viz., floor-dryers and tunnel-dryers.
The latter have the most extended application.

Floor-dryers. These may be of brick, heated by flues underneath them,
which conduct the heat from the fire-place at one end. Such floors are cheap,
but the heat is very unequal at the two ends, and the use of such floors
involves considerable labor in handling. Slatted floors, such as those used
for drying sewer pipe, may be used, but their cost of installation is great, and
the bricks also require much handling.

Tunnel-dryers. ‘The tunnels are made of brick or wood and heated by
hot air, steam or flues running under them. The bricks are piled on cars,
which are run on tracks into the tunnel. The cars are run in at one end
and always taken out at the other. The hot air is introduced at the end
where the bricks are taken out.

A recent improvement is the drawing of hot air from the cooling kilns
and blowing-it through the tunnels. Though still in the experimental stage,
this method will no doubt be widely used before long.

Burning. Paving brick are generally burned in down-draft kilns.
These are of rectangular or circular shape, the former having a capacity of
160,000 to 200,000 and the latter about 30,000. The rectangular ones are
quite generally used now, and it is only in a few districts that the manu-

facturers cling to the circular ones.

686 Reporr oF THE State GEOLOGIST.

Continuous kilns are used at several localities, and while they work
fairly well, still they can hardly be considered to have completely emerged
from the experimental stage.

In burning paving brick the temperature is gradually raised to the point
of vitrification and the kiln held at this temperature for several days in order
to allow the heat to thoroughly penetrate each brick and cause it to get its
maximum shrinkage. The kiln is then cooled very slowly to anneal the brick
and give a hard, tough product.

The temperature attained in paving-brick kilns varies, but it may be said
in general to vary from 1,700° F. to 2,000° F. In experiments made by
Professor Orton, Jr., of the Ohio Geological Survey, the temperatures of
paving-brick kilns when at their best heat varied from 1,800° F. to 1,920° F.
In the New York shales tested it was about 2,100° F.

Requisite Qualities of Paving Brick.

As paving brick are laid in streets, they are subjected to considerable
wear and tear, which they should be able to withstand if of good quality.
In order to determine by experiment in the laboratory whether a paying
brick possesses the requisite characters, certain standard methods of testing
have been devised.

Recently the National Brickmakers Association appointed a committee
to carefully go over the various methods of brick testing and draw up a set
of standard specifications. The tests considered were the rattler, absorption,
cross-breaking and crushing test, and the recommendations of the committee

were as follows:

Specifications for Abrasion Test.

LI, Dimensions of the machine. The standard machine shall be twenty-
eight inches in diameter and twenty inches in length, measured inside the
rattling chamber. Other machines may be used, varying in diameter between
twenty-six and thirty inches, and in length from eighteen to twenty-four
inches, but if this is done a record of it must be attached to the official report.
Long rattlers may be cut up into sections of suitable length by the insertion
of iron diaphragms at proper points.

IT. Construction of machine. ‘The barrel shall be supported on trunnions
at either end; in no case shall a shaft pass through the rattling chamber.
The cross-section of the barrel shall be a regular polygon having fourteen

sides. The heads and staves shall be composed of grey cast iron, not chilled

Ries—Puysicat Tests or Drvontan SHALES. ; 687

er case hardened. There shall be a space of one-fourth of an inch between
the staves for the escape of dust and small pieces of waste. Other machines
may be used having twelve to sixteen staves, with openings from one-eighth to
three-eighths of an inch between the staves; but if this is done, a record of it
must be attached to the official report of the test.

— LLL, Composition of the charge. All tests must be made on charges
composed of one kind of material at a time. No test shall be considered
official where two or more different bricks or materials have been used to
compose a charge.

IV. Quantity of the charge. The quantity of the charge shall be
estimated by its bulk and not by its weight. The bulk of the standard
charge shall be equal to fifteen per cent. of the cubic contents of the rattling
chamber, and the number of whole brick whose united volume comes nearest
to this amount shall constitute a charge.

V. Revolutions of the charge. The number of revolutions of a standard
test shall be 1,800, and the speed of rotation shall be thirty per minute. ‘The
belt power shall be sufficient to rotate the rattler at the same speed whether
charged or empty. Other speeds of rotation between twenty-four and thirty-
six revolutions per minute may be used, but in this case a record of the speed
must be attached to the official report.

VI. Condition of the charge. The bricks composing the charge shall be
dry and clean, and, as nearly as may be possible, in the condition in which
they were drawn from the kiln.

VIL. Calculation of the results. The loss shall be calculated in per-
centage of the weight of the dry brick composing the charge, and no result
shall be considered official unless it is the average of two distinct and complete

tests, made on separate charges of brick.

Specifications for Absorption Test.

1. The number of bricks for a standard test shall be five.

2. The tests must be conducted on rattled bricks. If none such are
available, the whole bricks must be broken into halves before treatment.

3. The bricks should be dried for forty-eight hours at a temperature
ranging from 230° to 250° F. before weighing for the initial dry weight.

4. The bricks should be soaked for forty-eight hours, completely
immersed in pure water.

5. After soaking and before weighing, the bricks must be wiped dry

from surplus water.

688 Report oF tHe Strate GEoLoacist.

6. The difference in weight must be determined on scales sensitive to

one gram.

j-
(.

The increase in weight due to water absorbed shall be calculated in

percentage of the initial dry weight.

Specifications for Cross-Breaking Tests.

1. Support the brick on edge, or as laid in pavement, on hardened steel
knife-edges, rounded longitudinally to a radius of twelve inches and _trans-
versely to a radius of one-eighth inch, and bolted in position so as to secure a
span of six inches. .

2. Apply the load to the middle of the top face through a hardened
steel knife-edge, straight longitudinally and rounded transversely to a radius
of one-sixteenth inch.

3. Apply the load at a uniform rate of increase until fracture ensues.

4. Compute the modulus of rupture by the formula

3) well
pit Se eerees
Ib=d?
in which

f = modulus of rupture in pounds per square inch.
mw — total breaking load in pounds.
/ — length of span in inches — 6.
4, — breadth of brick in inches.

d — depth of brick in inches.

5. Samples for test must be free from all visible irregularities of surface
or deformities of shape, and their upper and under surfaces must be perfectly
parallel.

6. Not fewer than ten bricks shall be broken, and the average of all be

taken for a standard test.

Specifications for Crushing Test.

1. The crushing test should be made on half bricks, loaded edgewise,
or as they are laid in the street. If the machine used is unable to crush a
full half brick, the area may be reduced by chipping off, keeping the form of
the piece to be tested as nearly prismatic as possible. A machine of at least
100,000 pounds capacity should be used, and the specimen should not be
reduced below four square inches of area in cross-section at right angles to

the direction of the load.

Rres—PuysicaLt Tests or Drvontan SHALES. 689

2. The upper and lower surfaces should be preferably ground to true
and parallel planes. If this is not done they should be bedded in plaster-of-
paris while in the testing machine, which should be allowed to harden ten
minutes under the weight of the crushing planes only before the load is
applied.

3. The load should be applied at a uniform rate of increase to the point
of rupture.

4. Not less than an average obtained from five tests on five different
bricks shall constitute a standard test.

It was resolved by the commission that “from the experimental work
done so far by the commission, or by others so far as is known to us, in the
application of the cross-breaking and crushing tests to paving brick, it is not
possible to show any close relationship between the qualities necessary for a
good paving material and high structural strength as indicated by either of
these tests.”

Extent of New York Shales, together with Tests of Samples from Type
Localities.

The shale bearing formations occurring in New York state, beginning

with that geologically oldest, are as follows:

Woweresrruriain oe ss ee Se Hudson river.

( Medina.
Clinton.
Niagara.

| Salina.

( Hamilton.
Wersecnet wen sed). gotten ke Les eee eo). oh Portage.

|
MMe meMMAN Sey scars gw ay fw A

nA
| Chemung.

Of these formations only the shales of the Salina, Hamilton, Portage

r utilized.

Oo
5

and Chemung are at present bein

Hudson river, This formation is abundantly displayed in the counties
of Lewis, Oneida, Montgomery, Schenectady and Columbia. Its tendency is
to exhibit siliceous or slaty phases, but m eastern Columbia county it becomes
at times argillaceous and at the same time contains considerable iron.

Medina. The Medina formation at times is shale bearing, as along the
Genesee river, where it is also marly, but the extent of the shaly layers is
unimportant. (Hall, Geology of the Fourth District of New York, p. 38.)
| 44

690 Report oF THE STATE GEOLOGIST.

The Clinton group is shale bearing in its lower members in eastern
Wayne county. It is a bright green shale and is about thirty feet thick. At
Sodus Point the shale is purplish. It occurs at other localities, but is very
thin, not more than two to four feet (Jd7d, p. 59.) The second green shale
of the Clinton group is less brilliant in color and everywhere full of fossils.
It is well exposed at Rochester and at Wolcott furnace, in the banks of the
creek, where it is over twenty-four feet thick. The shale is probably fre-
quently calcareous.

Niagara. Although a prolific shale formation in New York state,
the writer has not seen any exposures of it which were not either very sili-
ceous or calcareous, so that it would probably not work well for the manu-
facture of clay products. When ground and mixed with water it possesses
no plasticity.

According to Professor Hall (Geology of the Fourth District of New
York, p. 80), the Niagara shale forms a member of great development im the
lower part of the Niagara group. It is a dark bluish shale which, on expos-
ure, forms a bluish grey, marly clay. It is well shown at Lockport, in the
sides of the gorge at Rochester, just below the railroad bridge, and at many
localities in Wayne and Monroe counties. The lower layers of the shale are
less calcareous than the upper ones.

The followimg is an analysis of this shale, the sample taken from the
gorge at Rochester (Sixteenth Annual Report United States Geological

Survey, part IV, p. 569).

Silva, oy ee a, Lies ph geal eau pea ok ace ie oe On
Alramaiina< ys aca? gS eevee reel restate mete tot teh nee ae mea
Ferric Ox1d@,4:.1,- wan ot im ver eds lenin Rome ie uo nog eee mn ea
Lime, 3.24. oe shi etre ee ee ee ee
Magnesia, * .-t.3- 3 -abta. he tere) © oe «oil eee te yan mE
Adkahes:"-. Sai Rae Osta Ket ah here Pane he ain nner ae tick

76.16
H. T. Vulté, Analyst.

The shale is also to be found in many of the ravines and gorges, from
Rochester to the Niagara river.

Salina. The shales of this formation are contained in a belt extending
from Syracuse westward along the line of the New York Central railroad to ~

Riws—Pauysican Trsts or Devontan SHALES. 691

Buffalo. As a rule they are extremely impure and at times even marly.
They are soft shales, which weather very easily, and are generally red or
green in color and contain the beds of gypsum and salt.

The Salina shales are well exposed at Warners, near Syracuse, where
they are utilized for making brick.

Professor Hall says of the Salina or salt group (Geology of the Fourth
District of New York, p. 117), that it forms an immense development of shaly
marls and limestones, with interbedded deposits of gypsum. The formation
extends from Syracuse westward through southern Wayne county, and
northern Ontario and Seneca counties, northern Genesee and Erie counties
and a small part of the southern portion of Niagara. This group contains
important shale beds, although they are unfortunately very calcareous at
times and consequently require careful manipulation.

The red shale forming the lower divisions of the group was not observed
west of the Genesee river. It appears in eastern Wayne county, as indicated
by the deep red color of the soil overlying it. At Lockville the greenish blue
mar] with bands of red has been quarried from the bed of the canal. West
of the Genesee this is the lowest visible mass; the red shale has either
thinned out or lost its color, becoming gradually a bluish-green ; while other-
wise the lithologic character remains the same. On first exposure it is
compact and brittle, presenting an earthy fracture, but a few days are
sufficient to commence the work of destruction, which goes on till the whole
is resolved into a clayey mass.

The green marl of the lower division appears near the canal at Fairport
and again at Cartersville. The bed of the stream at Churchville shows the
greenish-blue marl.

“The prevailing features of the second division of this group,” says
Professor Hall, “are a green and ashen marl, with seams of fibrous gypsum
and red or transparent selenite. It occurs in the vicinity of Lyons and
numerous points farther west.”

The third division contains large gypsum beds and is probably not
suitable for use.

The Salina shale, as stated above, is worked at Warners, Onondaga
county, by the Onondaga Vitrified Brick Company.

The shale as exposed in their bank consists of a green or red, soft,
argillaceous shale, of considerable impurity as the following analyses
furnished by the company show.

692 Report oF THE Stare GEOLOGIST.

CALCAREOUS
LAYER IN BANK. RED SHALE. BLUE SHALE,
Silica tei <r atoeeee 25.40 52.30 57.79
Alpiminay career 9.46 18.85 Isao ba)
BieriG: OXI Cheese ane 2.24 6.55 5.20
ime, .2% ae 92.81 3.36 Onis
Magnesia Sings ae 10.39 4.49 4.67
Carbonic acid,. ... 20.96 3.04 3.42
Potash ea ae .95 4.65 Ay Gat
Od aa. oa eee 5 sah es) 1.22
Water and organic
IMabhers- =o. sateen 7.60 5:30 4.50
Coste L 99NS9 JOrme
Total fluxing impuri-
fies: ce eA PaTE 36.39 20.40 17.93

These shales must be quite fusible owing to their high percentage of
fluxing impurities.

At the works of the Onondaga Vitrified Brick Company, the shale
crops out in considerable thickness near the yard, and is of various shades
of red, green and some grey; it disintegrates very rapidly and the whole
bank is traversed by numerous cracks so that a small blast brings down
a large amount.

The material is mixed with a surface clay in the proportions of one
of clay to three of shale; it 1s ground in a dry-pan, and molded in an
auger machine; the green bricks are dried in tunnels and burned in circular
kilns; the product is of a light-red color.

Marcellus shale. This formation presents numerous undesirable features,
so that its occurrence is of little importance to clay workers. It is generally
slaty, gritty, and contains not unfrequently much iron pyrite and bituminous
matter. The rock is well exposed in the bed of the river at Le Roy.

As the Hamilton, Portage and Chemung are the most promising and
most extensive of the shale formations occurring in this state, a series of
physical tests was made on samples from several localities, to determine their
characters as related to each other and also as compared with other deposits.

The samples were ground to pass through a thirty-mesh sieve.* The

determinations made on these samples were: (1) Amount of water required

* Of most of the shales ground up by disintegrations, about sixty per cent. of any sample will pass through a thirty-mesh -
sieve, and the balance through a one sixteenth or an one-eighth inch mesh,

Rixrs—Pauysicat Trsts or Drvontan SHALES. 693

to make a workable paste, (2) shrinkage in drying, (3) shrinkage in burning,
(4) plasticity, (5) tensile strength of air-dried briquettes, (6) temperature of
incipient fusion, (7) vitrification, (8) viscosity.

The localities from which samples that were tested came, are Jamestown,
Angola, Hornellsville, Alfred Centre and Cairo.

Hamilton. The Hamilton is one of the great shale bearing formations
of New York state. It is also widely distributed, extending from the Hud-
son river to lake Erie, and at these two points shows wide extremes in its
lithologic character. In the east it is a true sandstone, in the west a clay
shale. “The valleys of Seneca and Cayuga lakes are both excavated, for
more than half their length, in the shales of this group.” (Geology of the
Fourth District of New York, p. 187.)

The Hamilton shales extend from Port Jervis northeastward along the
edge of the Chemung area in a belt about five miles wide, and then swing
westward from a point a few miles west of Albany, to Buffalo. In the
central part of the state the Hamilton belt is about twenty miles wide, and
thins to about twelve miles in the western half. The Finger-lakes are
largely bounded on the north by the Hamilton shale area.

Along the banks of Seneca and Cayuga lakes the full section of the
Hamilton group may be seen. The lower members are the most northern,
and dip to the south under the higher ones. Professor Hall makes the
following divisions:

1. Dark, slaty fossiliferous shale, resting on the Marcellus shale.

2. A compact, caleareous blue shale, of little thickness.

3. An olive or blue shale, which in its upper layers is stained by
oxide of manganese. This is one of the best adapted for clay products.

4. Ludlowville shales, often sandy in their nature.

5. A limestone.

6. Moscow shales, of greyish blue color, and slightly calcareous in
places.

These subdivisions can all be seen along the eastern shore of Cayuga
lake from Springport to Ludlowvyille.

Cairo, Greene county. This is the only locality at which the Hamilton
shale is mined. The material which is shipped to the works of the Catskill
Shale Paving Brick Company at Catskill, is a reddish gritty clay possessing
little plasticity. This material was at first used alone, but found difficult
to work on account of its excessive leanness, and consequently is now mixed

with fifty per cent. of common red clay also obtained from Cairo. Samples

694 Report OF THE STATE GEOLOGIST.

of this mixture were tested with the following results. The moderately
plastic paste shrank four per cent. in drying, and nine per cent. in burning.
Air dried briquettes had an average tensile strength of ninety-seven pounds
per square inch, and a maximum of one hundred pounds per square inch.

Incipient fusion occurred at 1,900° F., vitrification at 2,050° and
viscosity at 2,150° F.

The mixture of clay and shale is ground in dry-pans and then passes to
the pug mill on the floor above, whence, after tempering, it is discharged to
the auger side-cut machine. The bricks are repressed, dried in tunnels, and
burned in down-draught kilns. The company has recently erected a large
continuous kiln; in this kiln, most of the firing is done in temporary fire-
places built in the doorways of the kiln, no grate bars being used; it is
claimed that practically no fuel is charged through the small openings in the
roof of the kiln.

Portage. (See Geology of the Fourth District of New York, p. 224).
Another important shale occurs in this member of the Devonian formation.
The group consists of a lower shaly member, the Cashaqua shale, a middle
member of shales and sandstones, and an upper one of sandstones.

The Cashaqua shale is exposed along Cashaqua creek where it is a soft
green shale that weathers to a tough clay. It also occurs along Seneca lake
and at Penn Yan, but east of this becomes very sandy.

Good exposures are seen along Allen’s creek and Tonawanda creek, and
the branches of Seneca and Cayuga creeks. On lake Erie at Eighteen-mile
creek it is thirty-three feet thick, while along the Genesee river it is 150 feet
thick.

Concerning the Gardeau shales, Professor Hall states that they are
exposed along the Genesee river where the section involves alternating layers
of shales and sandstones. Toward the east the sandstones become more
prominent, but to the west, the shales increase and predominate so that along
lake Erie, “the Cashaqua shale is succeeded by a thick mass of black shale,
and this again by alternations of green and black shales” which aggregate
several hundred feet in thickness.

Angola, Erie county. The Portage shale is used by J. Lythe & Sons at
this locality for the manufacture of sewer pipe, fire-proofing, drain-tile, and
terra-cotta. The clay is somewhat less gritty than that at Jamestown. It is
a greyish, moderately coarse grained shale and contains scattered streaks of
bituminous matter.

Rires—Paysicat Tests or Devontan SHALzEs. . 695

When ground to thirty mesh it required 21.4 per cent. of water to make
-a workable paste, which was moderately plastic. This paste shrunk four per
cent. in drying and an additional ten per cent. in burning. The air-dried
briquettes had an average tensile strength of ninety-two pounds per square
inch, and a maximum of ninety-five pounds per square inch. Incipient fusion
occurs at 1,900° F., vitrification at 2,050° F., and viscosity at 2,200° F.

The analysis of the clay is as follows :*

RG er eee Sg el hehe se la tens SODaIS
Pe ELKO AMER OR k S oe Poe yaw A oo ce plenches - LOPS
CHIC CM MIUCMMEA REMC Ls a lic te Le y%. eh ireptedscws me n OO
nin Cua eid ee alee ee Ls | ae we ple yp a ) BDO
Retest A EMC Siar sl wc ashe Ss. ce ss 4. LD
POPES LUIGI! “Sep TG See gE BS RC |

Noval Hume nu Mes! <j yjre sti sbevselraiosticie”/ for (16294

In general composition it resembles a Carboniferous shale used for paving

brick at Kansas City, Mo.f This shows the following analysis:

aot nee RE RE ie ew er eee > «6BABT.
EN nan rN mentee ies ieleig ay cv say Soy) yath Sead! Ys clk Awe re p LOTS
Nicrai CMODMt GC mre RN ho re an, asic Meeiian wae wary GOT
VSS Ol Ook ae i Se a 82
VRRP ORT, on SE GR cris en EN ener ae a
Ole eae BT roe ee i lw B78
ics ral POUNDS eee GD we, chu c te © ye. ¥ otel LOOT

The principal output of these works is sewer pipe and fire-proofing. On
account of its softness the shale is easily mined and transported in cars to
the dry-pans, where it is first ground and then tempered in a wet-pan. The
tempered material is then conveyed to the upper floors and discharged into
the usual form of sewer pipe press. The glazing of the sewer pipe is done by
means of salt.

Chemung. The most southern shale formations of New York state are
included under this head. As a whole, the group consists of interbedded
shales and sandstones, the former prominent towards the west, the latter
becoming predominant to the east. The shales vary in color, and are black,

* Bulletin New York State Museum, III, No. 12, p. 228.
+ Clay Worker, December, 1893.

696 Report oF THE STATE GEOLOGIST.

olive or green. The shales sometimes pass into shaly sandstones, and these
are often highly micaceous. ‘The members of the group recognized by Pro-

fessor Hall, beginning at the top, are:

lon)

Sandstone and conglomerate.

Old red sandstone.

Grey and olive shales and shaly sandstone.
Green shale with grey sandstones.

Black, slaty shale.

Olive, shaly sandstone.

ro go Ro

_

Portage sandstone.

Of these members 2, 3 and 4 are the most important to clay workers, and
the beds of shale exposed are often twenty or thirty feet in thickness and free
from sandstone.

“On the Genesee river the shale is often in thick beds of a bright green
color and scarcely interrupted by sandy layers.”

“ Westward from the Genesee river there appears to be a constant aug-
mentation in the quantity of the green shale, which is often the predominating
rock, though from weathering to an olive color it does not always appear as
distinctly.”

“In the ravines in Chautauqua county, extending toward lake Erie, the
shale still retains its green color.”

Jamestown, Chautauqua county. This sample of shale came from the
bank of the Jamestown Shale Paving Brick Company.

This was a rather gritty shale, which required 18.5 per cent. of water to
make a workable paste; plasticity, lean. The paste shrunk 4.5 per cent. in
drying, and an additional 7.5 per cent. in burning, making a total shrinkage
of twelve per cent. Air-dried briquettes made of this mud had an average
tensile strength of sixteen pounds per square inch, and a maximum of twenty
pounds per square inch. This low tensile strength was due to the siliceous
character of the shale which, however, permitted rapid drying.

Incipient fusion occurred at 1,950° F., vitrification at 2,050° F., and
viscosity at 2,200° F. The clay burns to a deep red and dense body.

Alfred Centre, Alleghany county. Chemung shale is used at this locality
for the manufacture of roofing-tile. The shale is somewhat argillaceous, and
moderately fine grained.

It requires twenty-two per cent. of water to make a workable paste

which is slightly plastic. The shrinkage of this paste in drying is four per

Ries—Puysicat Trsts or Devonran SHALES. _ 697

cent. and in burning, nine per cent. The tensile strength of air-dried
briquettes was, on the average, sixty-one pounds per square inch, with a
maximum of sixty-two pounds per square inch.
Incipient fusion occurs at 1,900° F., vitrification at 2,050° F. and
viscosity at 2,150° F.
The composition of the shale according to an analysis furnished by the
Celadon Terra Cotta Company, of Alfred Centre, is:
Sec mee a ee Me RS LY Be OE BS OG
JE NSETTS STI OU 2

mmm HEE Tr Ol de a ke we a 1090

ere ae, ae ee Gea a 1.01
CSE Merk Ae ee eS SG .62
LON EGU Gi” Nols 22% ge NES a 2.69
SU UOEIAIG VEO, eee or 41
WE LONG EGG a 91
Sicnove Cerra he ee eS ke 6.39
MEseAMedG Oxides er sae ek sk ee 52

ORO U

locitusangmmpuriines: s a6 bs yetls) Goi. ier. B.A

‘This shale corresponds very closely in composition to that used at
Kansas city, Mo.,* for the manufacture of paving brick, but there is a
considerable difference in the fusibility, the Missouri shale being very fine
and consequently more fusible.

When this factory was first started, both terra-cotta and roofing-tile were
produced, but now the Celadon Terra-Cotta Company confines itself entirely
to the manufacture of vitrified roofing-tile, which is of a superior quality, and
bears an excellent and wide-spread reputation. At first a mixture of clay
and shale were used, but now the latter material alone is found sufficient ;
the shale after grinding and careful tempering is molded either by hand or
steam-power machines, and then set aside to dry slowly. The tile is no
longer burned in saggars as was formerly done, but is placed in pockets in
the kiln. The shale burns to a tough, cherry-red body.

Flornellsville, Steuben county. The shale at this locality frequently
contains interbedded layers of sandstone, which are separated in mining
without much trouble. The shale is rather gritty, and on the addition of

twenty per cent. of water gave a lean, workable paste, which shrunk 2.7

* Missouri Geological Survey, XI, p. 565.

698 Report oF THE SratE GEOLOGIST.

per cent. in drying and 5.3 per cent. in burning. The tensile strength of
the air-dried mud per square inch was on the average thirty-four pounds,
with a maximum of thirty-nine pounds.
Incipient fusion occurs at 1,900° F., vitrification at 2,050° F., viscosity
at 2,200°-K.
The shale burns to a dark red. It is used in the manufacture of paving
brick.
The composition of the clay, from an analysis furnished by the Hornells-
ville Brick Company, is as follows:
Silliead . cin, ce, Lon ha Be ko Sogo eae ene ee <a ap cee IE
Athumntnan.« > 28. sp a Sas a aa oe een 1

Ferric OxXI@@ Sate on Fe OLE a ee 7.04

TotGe<.4 se ee ee ; 58
Magnesia «0 doje 4 a-ha om ae a on angen eee

Potash so ce 2a Se ee eee ee ee

SROda "Lose dee iw Bee op ck ccna Mcgee an

96.16
Bluxes™ 2. soc fh3n ao 2k Be ah eet Sol ak ee ae ee eee

The method of manufacture followed at these works consists of the usual
dry-pan for grinding the shale and wet-pan for tempering it. The molding is
done by stiff-mud, side-cut machine, and the green brick are repressed. The
burning is in down-draught kilns.

From the tests cited above it will be seen that the shales used compare
very favorably with the requirements of a paving-brick material. Most of
them are slightly more siliceous than the average run of paving-brick clays,
but this 1s no serious objection.

The lean character of many can be overcome by the addition of plastic
clay, as in the case of the Cairo shale, in which instance the mixture, as
already stated, had a tensile strength of one hundred pounds per square inch.

The amount of fluxes present permits of their vitrifying at comparatively
low temperatures. But if necessary their refractoriness could be easily
increased by the addition of a certain amount of fire-clay.

Most of the shale deposits are easily accessible and located in close prox-

imity to railroads.

The Discovery of a Sessile Conularia.*

By R. Rurepemann.

In collecting, in a layer of the lower Utica shale, problematic filiform
fossils to which Professor J. M. Clarke had directed the writer’s attention, a
Conularia was found to which are attached several smaller cuneiform fossils
by organs which at first sight appear like rings. A thorough search in the
_ locality has furnished four more specimens of Conularia which bear such
appendages ; also a few impressions of shells of Zrochonema to which were
attached, in one case, a single individual of the supposed Conularia (PI. II,
fig. 1), and in another case many, but mostly poorly preserved, remains of
Conularia ; also the ever present Diplograptus foliaceus, Murch. sp., and the
above-mentioned problematicum, which will be described later.

That the Conularia, their cuneiform appendages and the similar larger
bodies attached to shells of Zrochonema belong together, is a supposition for
which this note is intended to submit the arguments.

The Conularie to which the supposed young are attached (Pl. I,
fig. it in which the interior cast of the shell is partly seen), as well as those
found without the young in the same layer, compare best with Conularia
gracilis, Hall.t This form was described from the shaly upper part of the
Trenton limestone near Middleville, N. Y., while the specimens of the writer's
collection were found in the lowest Utica shale.

One specimen (PI. II, fig. 5) has been figured on account of its remark-
ably well preserved ornamentation and the structure of the angular grooves.
It expands more rapidly than the others, the average angle of which is only
HOC SA specimen with a length of 14.3 cm. has an angle of 11°. The
specimen illustrated rests on one edge. This, however, is not the common
mode of compression in this species, for the great majority of specimens
apparently show only two angular grooves and one face of the pyramid,
because the whole shell has been compressed into the face on which it
originally rested. According to Holm} this mode of compression is found

with Conularie of quadratic section, while those of rhombic or rhomboidal

* Two instalments of this paper, with three of the accompanying plates, have already been published in the Asnerican
Geologist ; Article I, in Vol. XVI, March 1896, pp. 158-165, and Article II, in Vol. XVIII, August, 1896. pp. 65-71. The observa-
tions heretofore unpublished begin with page 711 of the present article, and are illustrated by an additional plate.

t Pal. of New York, Vol I, p. 224, Plate LIX, figure 5, 1847.

+ Sveriges Kambrisk-Siluriska Hyolithidx och Conulariide ; Sveriges Geol. Undersikning, Ser. C, No. 112.

701

702 Reporr oF THE STATE GEOLOGIST.

section are compressed in the direction of the obtuse angles. The shell of
C. gracilis Hall, which I have seen only strongly compressed, therefore
probably had equal faces and a quadratic section.

The complete flattening of the specimens without breaking, as well as
the common bending of the proximal parts of the shell (PI. I, fig. 4), are
indications of a slight flexibility of the shell. Hlall’s type also was “ slightly
bent or arcuate.” This remarkable character of (C. gracilis is causally
connected with the extreme thinness of the walls already observed by Hall.

As the observation of small wall fragments (Pl. I, fig. 6) and the

abundance of smooth casts of Conulariw indicate, the wall was very easily
destructible. This may also account for the frequent absence of wall remains
in the young Conularie while the edges are preserved. Plate I, figure 4,
and Plate II, figure 5, well illustrate this breaking out or dissolving of the
walls between the edges in even larger individuals.

The sculpture consists of “sharp, undulating, transverse strive and
scarcely conspicuous longitudinal ones.” (Pl. I, figs. 5 and 6.) The finer
longitudinal ribs alone, however, are continuous and the wavy cross-ribs con-
nect with them. Although the latter sometimes unite to form continuous and
very prominent cross bands, their whole appearance is such as to suggest that
they are wrinkles of shrinkage. The undulating transverse and the finer
straight longitudinal ribs are so characteristic a feature that they can safely be
used to distinguish this form from Conularia Trentonensis, Hall, C. Hudsoni,
Emmons, and C. guadrata, Walcott, which have straight and continuous
transverse ribs. The undulating transverse ribs are of special importance in
the study of the young Conuwlariw, as they are easily recognized by their
characteristic form whenever the surface film is sufficiently preserved,
however delicate it sometimes may be.

The cast of the mterior often shows, in different parts of the same
specimen, either the filling of the transverse ribs as similar ridges, or pustules
(cf. Pl. I, fig. 1) and deep furrows in place of the longitudinal ribs, or only
the latter, or in many places the cast is perfectly smooth. The last fact is
accounted for by specimens similar to that represented im Plate I, figure 4.
This interesting young Conularia, which at the distal end shows the straight

sulcate edges of a Conularia, has in the middle part preserved the wall which

consists of two layers—an exterior deep black, apparently carbonaceous one,
which shows the characteristic ribs of C. gracilis, and a much stronger inner
layer which has a more greyish, mineral appearance and is probably richer in

calcium phosphate. This second layer in the middle part between the two

RuEDEMANN—SEsSILE CoNULARIA. . 703

upper grooves, where it is apparently least crushed, is almost smooth, with
only an obscure indication of transverse lines of fracture. On the sides it is
broken into transverse ring segments. Although it is thicker than the outer
layer, it is more frequently lost, leaving, however, a smooth cast.

The segmental line appears as a shallow groove, scarcely conspicuous in
most specimens. It therefore is of no help in identifying the young Conu/laria,
Of greater importance in this regard is the structure of the grooves at the
edges of the pyramid, as this is generally the best preserved part of the fossil.
In the specimens, for instance, represented in Plate I, figure 4, and Plate
II, figure 5, the side walls of the grooves alone are preserved in the distal
part, the connecting wall being either dissolved, as indicated by the smooth
surface between the edges in Plate I, figure 4, or broken away as in Plate
I, figure 5. The walls of the grooves are much thickened, this strengthening
extending also to the adjoining parts of the faces, so that the grooves are lined
by two thick ridges. The connection between fragile thin faces and stout
edges seems to be found in other species also. Conularia Linnarssont, Holm,*
is described as having the grooves stronger than the segmental line and
being fragile toward the aperture.

As the original of Plate II, figure 5, shows at the upper groove, and as
has been observed in other species, the surface film extended—here with its
wavy transverse wrinkles—over the groove, covering and closing it (Pl. I,
fig. 2, @). Where the outer layer is lost, but the underlying parts are fully
preserved, there appears next below a thin smooth layer (4) with indications
of transverse lines of fracture ; this layer in its turn covers a milky white
laminated substance (phosphate of ime). The latter (¢) fills the groove and
contrasts strongly with the black shining walls (7). Often, however, this
substance is lost, leaving the groove empty or giving place to a filling by iron

oxides.’ The side walls of the empty groove show mostly very marked

transyerse fractures with upturned margins. The groove seen from the
inside (Pl. I, Fig. 3) has a roof-lke form with strongly slanting sides, which
are either smooth or exhibit the same transverse joints as seen from the
outside. Sometimes oblique pressure caused these joints to be pushed over
each other. Where the top is broken off the white phosphate of lime
appears again.

From these observations it may be stated that the edges of the pyramid
of Conularia gracilis, Hall, formed a kind of supporting framework for the

faces; that the grooves, therefore, had strong walls which were continuous

* Op. cit., p. 130, Plate IV, figures 38-40

704 Reporr of THE SrareE GEOLOGIST.

with the second mineral layer; that the grooves were filled with phosphate of
lime and covered by the sculptured outer layer with an underlying thin film
similar in appearance to the second layer. The groove, therefore, appears to
be altogether an expansion of the second layer of the wall. A diagrammatic
section of the groove at the angle of C. graci/is is given in Plate I, figure 4.

The reasons which the writer has for regarding the cuneiform appen-
dages of C. gracilis, and the bodies attached to Trochonema, ete., as remains
of young individuals of C! gracilis are as follows :

1. Wherever an appendage is preserved completely it shows four
divergent grooves, such as would form the edges of a pyramid, with about
the same angle as the older shells of C gracilis (Pl. I, figs. 2, 3, Pl. HU,
tie

or

x. 1). Some apparently show only three grooves, but investigation will
generally bring out the fact that the fourth is divergent from the plane of the
others and hidden in the matrix. Generally, however, the whole fossil
appears only as a cuneiform film between two thick edges, which are formed
by two coinciding grooves, while the two originally vertical faces have been
folded inward between the horizontal ones or partly bulge out from between
them (Pl. I, fig. 1, @). Some appendages show even but one groove;
the proximal parts of the other grooves, however, are also ordinarily traceable
into the matrix (PI. I, fig. 2). It is to be concluded from this that the
complete appendages contained grooves which originally did not lie in one
plane.

2. The four grooves show exactly the same structure and composition
as those of C gracilis, 1. e., the V-shaped section, the filling with milk white
phosphate of lime, the extension of the carbonaceous sculptured surface film
over them, and especially the very characteristic and easily discerned trans-
verse ridges of the side walls of the groove. (Cf. Pl. I, figs. 1, 6, 2,5;
Pl, ties 79)

3. The space between the grooves of the appendages is generally
perfectly smooth, thus indicating that between them was a connecting wall
which is now lost. However, in many places the tender carbonaceous surface
film is still preserved. Where this is the case the longitudinal ribs, as well
as the characteristic undulating transverse wrinkles, are clearly discernible, as
indicated in Plate I, figures 1, 2, and Plate I, figures 1, 7, at s.

4. The carbonaceous cup-shaped bases, by which the supposed young
Conulariw are attached to the older individuals, are exactly similar to those
of some larger fossils which can be safely referred to C. gracilis, and

especially similar to the basal cups of the two important specimens repro-

RuEDEMANN—SESSILE CONULARIA. j 705

duced in, Plate I, figure 4, and Plate Hl, figure 1. The latter, which on

{ the four grooves and the

account of its general form, the structure o
sculpture of the surface film, must be regarded as identical with, or very
closely related to C. gracilis, has a beautifully preserved cup of the same size
and structure as those attached to the original of Plate II, figure 2.

5. Finally, it may be adduced as an additional argument for the
similarity of the observed appendages and the shell of a Conularia, that in
some of the former (Cf. Pl. I, fig. 1, ¢) a triangular subcarbonaceous plate
is preserved which is strongly suggestive of the flattened apertural process
of the uppermost face.

It is permissible to meet some of the objections which are easily sug-
gested in comparing the appendages with Conularia. There is first the
strangely curved form of many of the smaller and medium sized individuals.
As already stated, Hall’s type, of about two inches in length, is “slightly
arcuate.” The axes of the older specimens, however, which the writer pos-
sesses, as also the axis of the specimen figured in Plate II, figure 5, are
always perfectly straight. An examination of the shells of the young Conw-
laria establishes the fact that the better they are preserved the straighter
they are. (Cf. Pl. I, figs. 1, 2.) Even some of the very smallest Conu-
larie are straight. ‘This, as well as an examination of such specimens (PI. I,
fig. 4), im which the youngest part only is bent and the older is perfectly
straight, leads to the conclusion that the young shells also of C. gracilis were
straight, but probably more flexible than the more distal parts and perhaps
less able to resist the dissolving influence of the sea water. A group of fos-
suis (Pl. H, fig. 7) which are attached to the poorly preserved cast of a
Trochonema shell, on account of the strong distortions of the wedge-shaped
appendages presents appearances differmg most widely from those of Conu-
lavia. In this case the appendages are identical with the leaves of Hall’s
Sphenothallus angustifolius.* The extensive destruction of the faces of the
pyramids in both specimens, as well as the very poor preservation of the gas-
tropod, is proof enough of the destructive influences to which they were
subjected and which may also haye distorted the slender pyramids before
they were covered by sediment. On the other hand, both contain a sufficient
number of nearly straight shells (cf. especially Hall’s figure) to warrant the

statement that the pyramids were originally straight. The writer’s specimen

* Palaeontology of New York, Vol. I, p. 261, Plate LX VUI, figure 1, 1847. _Hall’s type, whichProfessor J. M. Clarke had the
kindness to lend the writer and which is figured on Plate TV, not only shows young individuals attached to older ‘‘leayes,”’ but
also ring-like impressions of the basal cups and the transverse ridges of the grooves. The faces have left smooth impressions
only

45

706 Reporr or tHe Srare GEOLOGIST,

exhibits besides, in several places, well preserved transverse undulating cross-
ribs which are very similar to those of C. gracilis.

Another objection, which naturally arises in studying these forms, is this;
assuming that other Coniwlari@ were sessile also, why have not any such
bases been found among the thousands of specimens of the species already
described? Barrande had more than a thousand specimens of certain
species without noticing such basal cups in the young, which are generally
stouter and better preserved than any other part of the fossil.

In almost all described shells of Conulari@ the apex is broken off, either
irregularly or along a septum. The irregularly broken shells, which compose
by far the great majority, have undoubtedly lost their proximal parts and are
therefore not complete and may be considered out of the discussion. Those
closed by a septum are most probably not complete either, for as Dr. A.
Ulrich* has pointed out, the empty chamber between the imperforate septa
must have been more liable to destruction than the other sediment-filled part.
It may, therefore, have. been lost in most cases, and only that part of the shell
beginning at the youngest septum may have been left to us. It remains in the
extremely small number of fully preserved shells. Wiman,t on the basis of
Holm’s paper, estimates their number at less than 5.55 per cent. of all known
Conularie. ‘These few forms again, although tapering down to a very small
diameter (the writer does not know of a real “ point” having been observed),
do not exclude the possibility of having been expanded again into a base. It
is true that it does not seem very natural to have a large pyramid supported
by such a thin stem, but this was, in fact, the case with rather large shells of
C. gracilis (Pl. Il, figs. 1, 7). Suppose all Conulariw were attached thus,
then it would have been just as strange 1f the pyramids, in becoming covered,
had not been broken right over the bases, as it is that not more of the shells,
if they were free, should have preserved the apex. It also bears on this ques-
tion that several cups, among them one with a diameter of 5 mm.; have been
found which bear only a very small fragment of the pyramid (PI. III, fig. eas
and that the specimen represented in Plate I, figure 1, bears a great number
of bases from which the young Conularia are broken off. The preservation
of the apex not only forbids any positive conclusion as to the mode of life of
the Conulardw, but the supposition of their free existence seems to be question-
able and will, therefore, be discussed hereafter.

As none of the large specimens of C. gracilis have been found attached,

the question as to mode of life can not be directly answered. It can, however,

* Palwozoische Versteinerungen aus Bolivien, p. 35, 1892
+ Palwontologische Notizen 1 und 2, Bull. Geol. Inst. Univ. Upsala, Vol. IT, No. 3, p. 7, 1894.

RuEDEMANN-—SESSILE CONULARIA. 707

be remarked that the largest specimen in the writer’s collection (length 14.3
cm.) is preserved to a breadth of 4 mm. and ends in a deep impression which
could be caused by a cup not larger than the largest well preserved one which
has been found. Further, it will be noticed that some of the attached shells
(Pl. IV, fig. 40; Pl. II, figs. 1, 7) have already reached a size which renders
it improbable that the enclosed animals should still have changed their
mode of life.

After having presented the general features of the occurrence of a sessile
Conularia, the writer intends now to describe the most novel part of the
fossil, 7. ¢., the basal appendage.

Though an attempt to isolate and decolor some of the appendages failed,
partly on account of an obscure cleavage in the rock and partly on account of
the consistency of the residuum after the treatment with acetic and hydro-
fluoric acids, the author succeeded at least in developing, by the application
of the same agents, several of the stout chitimous appendages on the slabs
(cf. Pl. IU, figs. 5 and 16). The defects in the preparation of the material are
atoned for by the well-preserved state of the material itself, for several of the
bases are preserved in neat natural sections (cf. Pl. IL, figs. 2 and 3), a com-
parative study of which, as well as of the varying aspects of the other bases,
allows a fair insight into the structure of this interesting organ. In order
to énable the reader to form for himself a picture by a comparison of
the different states of preservation, the writer has given as many sketches as
possible.

As already stated in the first article, most bases appear at first sight as
stout subcircular to suboval chitinous rings* (cf. Pl. IL, fig. 1, which is the
base of the specimen reproduced on Pl. IH, fig. 1). The original form was
probably circular, as the elongated forms (cf. Pl. III, fig. 20) are generally
found near the edge of the supporting fossil (cf. Pl. I, figs. 1 and 2),
where they were more liable to become laterally compressed than those on the

inner part of the fossil.

* These rings were observed by A. G. Nathorst as early as 1882 (cf. A. G. Nathorst, ‘*Om férekomsten af Sphenothallus
cfr. angustifolius, Hall, i silurisk skiffer i Vestergétlana” in Geologiska Féreningens i Stockholm Férhandlingar, Vol. VI, p 315,
Pl. 15). The same author has published in the April (1896) number of the same journal (Vol. XVIII, No. 4), under the caption,
“ Sphenothallus en Conularia,”’ areview of the study of this interesting fussil in Sweden, from which it appears that he, in
describing, in the first cited paper, a specimen of Sphenothallus, Hall, from the Silurian shale in the neighborhood of Vamb in
Westgothland, accepted Hall’s interpretation of the fossil as an alga. Some years later, however, another specimen was sent to
him by Dr. N. O. Holst, the state cf preservation of which wassuch as to convince Nathorst at once of the impossibility of
referring the fossil to the vegetable kingdom. He pointed out this fact to Holst, who afterwards sent the same specimen to J.
Chr. Moberg for identification. The latter reached the same conclusion, as appears from an extract of a letier of his to
Nathorst: ‘‘It seems to remind me somewhat of a Conu/aria, and above allit surely was not an alga.’ Nathorst himself vow
accepts the identification of Sphenothallus with Conularia. Hall's type is not so well preserved as to have been able to suggest
a comparison with Conularia.

708 Report oF THE State GEOLOGIST.

The dimensions of those rings. which are found still attached to a Conu-
laria ave: Diameter from 1 to 2 mm. (original of fig. 1, Pl. III, measures
1.3x.7 mm.; original of fig. 19, Pl. III, 1.75x2 mm.), though a few larger
separate ones have been found (one measuring 4 mm.); height .8 mm. (taken
from the originals of figs. 1, 2 and 3, Pl. IIT).

Externally the ring is perfectly smooth and shining (fig. 1), expanded
more or less abruptly towards the base (cf. Pl. III, figs. 2, 3, 18, 18). Under-
neath it possesses a system of regular radial folds (cf. Pl. III, figs. 7, 8, 9, 18,
18). The true nature of the rings is revealed by a few vertical sections which
were found on some slabs (cf. figs. 2 and 3). Figure 2, Plate III, is a repro-
duction of the whole fossil, which is interesting because it demonstrates not
only the occurrence of basal appendages detached from the extraneous object,
but also the common separation of the pyramid of Conularia gracilis from the
appendage a little above the latter. As both sections are not quite median,
part of the rig is seen from the inside. In both, the ring becomes attenu-
ated toward the top (in fig. 2 abruptly), thus forming a skin which fastened
the basal appendage to the pyramid. This skin formed a dome above the ring,
as may be inferred from the laterally compressed specimen reproduced in fig.
9, at a; bis the basal rmg, which on account of its bulging out a little more,
adheres to the counter part of the fossil. The general form of the appendage
may be compared to a bell, which term will be apphed in this paper to the
exterior chitinous wall of the organ under consideration, as the word does not
imply any expression regarding the possible functions of the whole.

Figure 10, Plate III, reproduces a specimen (taken from the original to
Pl. I, fig. 2), which gives a view of the imside of the dome of the bell and
exhibits irregular radial wrinkles of the skin, caused probably by shrinkage
prior to fossilization. In figure 12 a base is seen from above. Here the
greater part of the ring is preserved, while the upper portion of the bell left
only its impression.

As appears from figure 8, Plate HI, which reproduces the view allowed
by one of the appendages into the bell from beneath, the latter, or at least its
thicker basal part, consisted of: concentric layers.

The absence of any carbonaceous film at the base of the bell (cf. figs. 7, 8,
13, Pl. IIT) would lead to the conclusion that the bell was open there: but
the smooth surface of the rock inside of the deeper impression of the ring
(cf. fig. 97) in several specimens indicates the former existence of a basal
closing film. A very clear view of the latter is furnished by the basal

appendage (cf. fig. 15) of the Conularia reproduced in figure 14, which

RuEDEMANN—SEssILE CoNULARIA. 709

apparently was attached to a little fragment of a Stictoporella. It appeared at
first like figure 15; the dissolving of the enclosed rock, however, brought out
the entire base of the organ, namely, the broad, deeply-impressed exterior ring
(a), the impression of the somewhat wrinkled film (4) stretching towards the
center of the base and connecting with an internal part (c) that appears as a
narrower, radially furrowed impression of a ring. The latter can be seen very
distinctly at the bottom of the basal appendage reproduced by figure 1. In
the remarkable specimen belonging to figure 6, all chitinous parts have been
removed by weathering except two stout rings, which strongly contrast with
the buff-colored weathered shale, and which are evidently the bases of the
bell and of an internal part of the appendage. The original of figure 5
(taken from the group Pl. II, fig. 7) exhibits also a stout, though now,
through the action of the acids, somewhat corroded ring. Another
reproduction (fig. 7, Pl. HI) of the underside of a basal appendage shows the
latter removed from the center, apparently by the overturning of the young
Conularia to which it was firmly attached. It is partly preserved in the
original of figure 9, Plate III, and it can be distinctly seen in the basal
appendage reproduced in figure 13, Plate iI (taken from the group Pl. I,
fiz. 5), where it stands out in relief, while its system of basal radial furrows
can be seen in figure 18 at 4,

- The real form of this internal body is revealed by a fine vertical section
through the basal appendage (fig. 3) of a detached Conularia (fig. 4, Pl. 111).
This section shows again a crescent-shaped cleft of a stout chitinous body,
proceeding from the converging marginal grooves of the pyramid of Conularia.
The horns of the crescent can be traced to the chitinous mass of the basal
ring of the bell, the inside of which is visible in the section. The original
of figure 5 assists in making evident that this crescent is the section of
a chitinous cup-shaped body, which is fastened to the apex of the pyramid,
while its base is continuous with the basal skin, extending to the exterior
bell. The cup itself was not closed basally, as can be inferred from the
little node in the center of the impressions of the basal appendages (cf. fig.
9d).

It remains to consider the connection of the pyramid of Conularia with
the basal organ. As the sections figures 2 and 3 indicate, the angular
grooves of the pyramid curved in at the basal end. The subquadrangular
piece broken out of the dome of the bell in figure 10 suggests that the shell
of Conularia yet retained its quadrangular section when entering the bell.
The counterpart of this fossil (fig. 11) has preserved the broken-out chitinous

710 Report OF THE STatre GEOLOGIST.

piece and exhibits on the latter a cross of four ridges, consisting of pyrite. A
similar aspect is presented by the node in the middle of the basal appendage
of figure 17, Plate III, which is an enlargement of the base of the specimen
reproduced on Plate I, figure 4, and which shows two arms and the intersec-
tions of the two others on top of the central node. The pyrite in both specimens
points to the former existence of canals, or at least to an original difference
between the material which has been replaced by pyrite’ and the enclosing
chitine. There can hardly be any doubt that the cross of pyrite represents
the basal junction of the marginal grooves of the pyramid, and that the little
node in the center of the base (cf. figs, 11 and 17, Pl. IID) is the real apex of
the pyramid. The direct continuance of at least two grooves is exhibited
by quite a number of remains, e. 7., by those reproduced in figures 18 and 19,
while the original to figure 20 gives a neat section through the four grooves
at the entrance of the pyramid into the bell. It is evident from the latter
fossil that these grooves, as already demonstrated, were originally covered by
a carbonaceous film and filled with phosphate of lime. The supposition is,
therefore, not out of the way, that they may have been free from this filling
towards their proximal ends and could therefore have been filled by pyrite
during the process of fossilization.

The morphology of the whole appendage will be best understood from a
diagrammatic section, as given in figure 21, Plate JI]. The apex of the pyra-
mid (@) is enclosed in a stout central cup (/) which, in turn, is connected by
a thin film (¢) with the broad basal extension of the exterior bell (@). The
latter again is fastened to the pyramid a little above the cup.

There can be no doubt that the basal appendage was an organ of
attachment. It is further evident that the latter did not amount to a
coalescence, but was of a temporary character only; for the not uncommon
occurrence of detached specimens with well-preserved basal appendages (cf.
figs. 2 and 4) is not consistent with the assumption of a coalescence. The
apparatus, therefore, can not be compared to the basal disks, such as certain
bryozoans have. On the other hand, it is indicated by the impressions left
by the appendages* that their inner parts were flexible or even retractible
while the stout exterior bell, with its broad, radially striated base, apparently
served to give stability to the mechanism and to close the interior tightly
from the exterior.

An attempt to compare the basal appendages to suckers, such as various

gastropods use for purposes of attachment, would lead to the further

* Of. figs. 9 and 16, which show the ring- like impression (¢) of the bell to be considerably deeper than that of the wrinkled
basal film (qd).

RuEDEMANN<—SESSILE CoNULARIA. Fatal

assumption that their interior was filled with muscular tissue, and con-
sequently connected with the circulatory system of the living animal. The
writer was unable to study this question on account of the negative results
which followed his attempts to isolate the appendages; neither did he
succeed in tracing the confluent canals, indicated by the cross of pyrite at the
apex of the shell, which may have effected a connection with the interior of
the pyramid and thereby have become instrumental in producing a vacuum
by the withdrawal of a fluid, similar to that found in the pedicels of the
echinoids. The writer, however, is inclined to suppose that there existed no
connection whatever between the interiors of the pyramid and of the
appendage, but that attachment was effected by the elasticity of the latter
alone, especially by that of the central cup. The organ might then be
compared to the chitinous suckers with which the males of certain water-
beetles (e. g., Hunectes) are provided, and which possess no muscular tissue
whatever but adhere to foreign bodies by external pressure and by sub-
sequently resuming the original shape through their own elasticity, thus
producing a vacuum much like the India rubber plates which are used to
fasten objects to the glass panes of show windows. The shape of the central
cup as well as the fact that the appendage consists of a substance which
certainly was elastic, could be adduced in favor of this supposition, while
there seems to be no serious obstacle in the way of assuming that the animal,
which no doubt had a certain power of free moving, had the further
power of pressing the apex of the shell and with it the securely fastened cup
to the body it wished to adhere to.

The diagrammatic section, figure 21, Plate III, is intended to illustrate the
working of the apparatus, the dotted part representing the latter in the
state of compression preparatory to attachment, and the striated part shows
the same in the state of attachment by suction.

It should be remembered that however erroneous the attempt to explain
the special operation of this organ may be, this does not affect the fact that
the attachment was evidently only a temporary one and that the impressions
left by the appendages show both the connecting film and the central cup
bulging inward. These observations can, in the opinion of the writer, be
only accounted for by the assumption that the basal appendage was an organ
of attachment by suction.

The publication of the concluding part of this article on Conularia
gracilis, Hall, has been much delayed because of a fortunate discovery
during the past summer (1896) of a locality on the bank of the Bast

Tale Report oF THE STATE GEOLOGIST.

Canada creek, which yields specimens of this Conularia uot larger than .5
mm. in length, and which, therefore, enables the author to furnish some
further details relating to the development of the shell of this interesting
animal (cf. Pl. IV). The minute, oval, carbonaceous bodies cover some of
the layers in astonishing multitudes.

While the great majority of the tiny fossils are found promiscuously
scattered over the slabs, some of the latter, otherwise poor in such detached
specimens, bear linear carbonaceous films, with outlines so straight and well
defined as to make it improbable that the film should be the result of an
accidental drifting together of shells. One of these bodies has been reproduced
in figure 1, Plate IV, on account of the distinctness with which it shows its
composition of young shells of Conularia. There are others of more regular
outline, the most complete of which attains a length of 31 mm. and tapers
regularly from a width of 5 mm. at one end to 4 mm. at the other. This film
consists of minute shells of Conu/aria, which become especially distinct at
both of its ends, where it is more or less lacerated. ‘The shells observable
in these films range in length from .5 mm. to 2 mm. <A few specimens
(cf. fig. 2) have been collected, which indicate that the shells were sometimes
regularly arranged and attached to some central body, which, in the orginal
of this figure, is not preserved. Whether these probably originally cylin-
drical aggregates of spawn of Conularia are brought about by the crowded
fixation of young individuals around extraneous bodies, as ¢. g., fragments of
seaweed, which are not preserved, or whether it is a case of brood-protection,
has not been ascertained with the material thus far collected.

There can, however, be no doubt that the animals, in the infantile
condition which comes under observation here, were already seeking attach-
ment to other bodies, in spite of their usual irregularly scattered
occurrence on the slabs, which might suggest a swimming habit. This
is clearly shown in very youthful stages found attached to little cones
(probably belonging to a Monticulipora), which project from the slabs
(cf. fig. 3), and above all by the possession of the organ of fixation, namely,
the basal appendage.

There have been no shells found which did not reach a length of .56 mm.,
while fossils between .56 mm. and 1 mm. are quite common. This smallest
stage obtainable (cf. figs. 4 to 7, Pl. IV), is characterized by the presence, and
relatively large size of the basal cup, which attains half the size of the entire
shell; by the apparent greater breadth and by the curved outline of the

living chamber, which often approaches a circular shape.

RuEDEMANN—SEsSILE CoNULARIA. 713

The distal margin of the shells is composed of small denticles which
develop into the apertural processes of the adult stage. In all the broader
specimens there terminate, between these denticles, longitudinal lines, which
are of darker color than the other film and which divide the latter in sections
of equal size (cf. figs. 5, 7,10, Pl. IV). They are, as shown by their position,
the first indications of the marginal grooves observable in this early stage.
The appearance of several of these denticles and grooves cn the broader speci-
mens indicates that the apparent great breadth of the youngest stage is
largely due to a complete flattening. This explains also why a few specimens
have been found the marginal angle of which is not much larger than
that of adult forms (cf. figs. 8 and 9).

Such abruptly broadened shells as that reproduced in figure 6 are a
common occurrence. It is obvious that in this case the shell burst at this
point and became subsequently more distally unfolded.

Even larger shells, though by far not so common as those of the smallest
stage, were subjected to bursting and spreading in one plane. Figures 17, 18,
25, 28 and 31, Plate IV, are taken from such specimens. The crushing
sometimes led even to a separation of the faces, as in the original of figure
11. The infrequent observation of adult specimens of Conularia which are
complete, in comparison to the profuse occurrence of fragments of faces,
may be largely due to such separation of the faces before becoming covered
by sediment.

A remarkable feature of many of these minute shells is the darker
appearance of the basal appendage when compared with the living chamber.
Shells where this difference is especially noticeable are reproduced in figures
5and 7. This difference can, no doubt, be accounted for by the different
thicknesses of the chitinous walls, and this is also indicated by the less com-
pressed condition of the basal appendages in more advanced stages (cf. Pl.
PVimies, 127 135° 14,:18, 22, and especially Pl. I, figs. 2 and 5; Pl. II, fig. 1).

Increasing in length, the shell generally becomes more slender in shape
(cf. Pl. IV, figs. 13 to 32), though specimens with oval outlines are by no
means rare (cf. figs. 17,21, 29). In looking over the slabs with the naked eye,
it will even seem as if all the tiny fossils consisted of carbonaceous oval bodies
with a dise or ring at one end. The glass, however, will in the majority of
the specimens reveal straight margins (cf. fig. 26) and a truncated (cf. fig.
21) or acute (cf. fig. 30) distal end.

The relatively large size of the basal appendage in the smallest forms has

already been mentioned. Though in these smallest specimens the details of

714 REPORT OF THE STATE GEOLOGIST.

the basal cup could be discerned only in exceptional cases (cf. fig. 12), it at
once becomes apparent in somewhat larger specimens that the appendage
differed only in size from the organ previously described. Figures 11 to 34
illustrate sufficiently the various aspects, and also the somewhat differing size
which the appendages show according to their state of preservation and the
direction and amount of their compression. The specimens which exhibit the
underside of the base (cf. Pl. LV, figs. 12, 18, 21, 22) show plainly its radiated
surface. Others give lateral views of the appendage (cf. figs. 4, 9, 10, 11, 18,
19, 28, 24, 26, 27, 28). Of these the original of figure 10 is especially imter-
esting. This has apparently. preserved the protruding interior cup; that of
figure 15 plainly shows the ring-like thickening of the basal part of the exte-
rior cup. Some specimens even present sections of the base (cf. figs. 8, 16,
17, 32, 33), while the majority of the appendages, which appear as solid,
smooth discs (cf. figs. 5, 7, 29, 80) evidently expose the upper side to view.

While most specimens terminate in triangular outlines, undoubtedly
formed by the apertural processes In an expanded state, numerous shells
present at first sight a somewhat puzzling aspect by the appearance of a well
defined, often darker, and somewhat projecting square plate or of a corre-
sponding impression, at the distal end (cf. Pl. LV, figs. 13, 19 to 22, 32). As in
several specimens the composition of this plate of four triangular pieces could
be observed (cf. figs. 19, 21, 22), it may be safely inferred that, by an
obliquely lateral compression, the summit aspect of the fossil has been pre-
served and all four apertural processes are visible. A complication of this
aspect is often caused by the appearance of a central circular impression
which is surrounded by one or more concentric ridges (cf. fig. 20). The
writer is disposed to regard the latter as parts of the internal shell-wall which
have been pressed through the apertural plates. This assumption pre-
supposes that the terior section of the shell was not quadratic but circular,
a supposition which seems to be supported by the occurrence of examples
which show a well defined circular spot in the center free from carbonaceous
matter (cf. fig. 23).

Indications of a surface sculpture are extremely rare in the great
majority of infantile specimens. All that can be seen in the smallest speci-
mens Is, now and then, a series of distant transverse furrows (cf. Pl. LV, figs. 6,
14, 24, 25), which would seem to belong to a deeper, transversely fractured
layer, such as has been observed in the original of Plate III, figure 4. The
original of figure 26, Plate IV, shows a fine longitudinal striation and that of

figure 27 exhibits at the distal end distinct longitudinal ridges and slight indi-

RvuEDEMANN—-SEssILE ConvunarRiA. 715

cations of transverse ridges which suggest a comparison with the surface
sculpture of the adult Conularia. As these few indications of surface sculp-
ture in the smallest stages are, however, in contrast to the generally smooth
appearance of the fossils, they can hardly be regarded as reliable evidence of
the existence of a sculpture in this smallest stage, and may be only secondary
corrugations. There has, however, been found a specimen, 4 mm. long,
which is excellently preserved and which exhibits a system of distinct
intersecting longitudinal and transverse ribs (cf. Pl. IV, fig. 35). The sculpt-
ure of this fossil differs from that of an adult individual in the appearance of
the transverse ribs which are not undulating but straight, and which, towards
the base, become more prominent than the longitudinal ones. The same
speciinen possesses a peculiarity in its four deep transverse furrows. Whether
the latter originate from more closely arranged transverse ribs and retarded
growth or from the former presence of septa which are broken out, remains
doubtful because of lack of corroborating observations.

Adolescent stages ranging in size between the last described and the
adult stage, have been described and figured on Plate I, figures 1, 2, 3, 5.
They show the sessile mode of life of these stages, the structure of the basal
cup, the presence of the surface sculpture which is characteristic of Conularia
gracilis, and the peculiar transverse ridges of the side walls of the marginal
grooves.

All the forms described so far are flattened, often into a mere car-
bonaceous film and can not be regarded as giving conclusive evidence as to the
transverse section and actual general aspect of the infantile shell. This
defect in the material has been filled by a single fortunate discovery of a
small slab bearing eight young Conularias which are either not at all or but
slightly compressed. Two of the latter (cf. Pl. IV, figs. 837 and 38) were
attached to a shell of Andoceras. Most of these shells, as well as the impres-
sions of some which are broken out, are perfectly round (cf. figs. 86 and 38)
and remarkably strong. The position of the marginal groove is indicated by a
narrow furrow. They are perfectly smooth, but as indicated by one specimen,
a sculptured superficial layer existed originally around the thicker interior
shell. Figure 37 is taken from a specimen which suffered a shght crushing;
as a consequence, the median part is sunken in and the stronger marginal
grooves appear as a projecting frame, giving also to this form the appearance
of a compressed pyramid. While this specimen explains why even very
young shells may appear as pyramids, it is shown by the uncompressed

specimens that the original section of the youngest stage was circular. The

716 Report OF THE STATE GEOLOGIST.

writer already has had occasion to observe the round section of the basal part
of larger specimens before this material was found (see Pl. I, figs. 3 and 4),

and the concentric furrows on the apertures of flattened specimens, which.

were mentioned above (cf. Pl. IV, fig. 20), point to the same fact.

It may be concluded from these observations that the young shell of
Conularia gracilis consisted not only of the thin sculptured surface layer but
also of a thicker carbonaceous interior layer. The interior surface of the
living chamber, formed by this latter, was smooth. This can be seen
wherever the cast only of the shell is preserved, as for instance in the original
of figure 40, at 4. The cast consists of four smooth faces extended between
the marginal grooves.

The uncompressed specimens show further that the young shells were,
in fact, much more slender than the compressed fossils would suggest. They
often approached at the basal end more to a cylindrical than a conical shape,
an observation which is illustrated in the above mentioned figures of Plate I
(figs. 3 and 4). The latter figure also shows well the gradual change of
the cylindrical young shell into the pyramidal form by the marginal grooves
becoming more prominent. There is no doubt that the marginal grooves were
present in the incipient shell, for this is proved by the originals of figures 5,
7, 10, ete. (PL IV), but they were only part of the superficial layer, as shown
by the specimens belonging to figures 36 and 38, and became important only
in the thinner later part of the shell.

The writer has added to these illustrations that of a fragment of a shell
which plainly shows a convex segment at the apex (cf. fig. 39). It naturally
can not be decided from a single specimen* whether this shell accidentally
broke at the segment or whether we see the result of a discarding of the basal
appendage by the adolescent animal. It is worth mentioning in regard to the
latter possibility that the writer made only one other observation which
might indicate the existence of septa in Conularia gracilis, namely the above
mentioned constrictions of the original of figure 35, Plate IV.

Finally, a reproduction of the type of Sphenothallus angustifolius, Hall, has
been added in figure 40, in order to indicate the traces of basal appendages,
which are perceptible, as well as two young shells attached to a larger one at
a. A part which is of interest in regard to the conception of the shape of
Conularia is marked 6. The upper face of the pyramid is here broken away,
whereby the crushed lateral faces and the opposite lower face are laid open.

The section of the cast is broadly rectangular.

* The apex of the original of Plate II, figure 5, is not distinct enough to be of account.

;
;

RuEDEMANN—SESSILE CONULARIA. Ta

The general conclusions which can be inferred from the preceding
observations are the following :

1. The smallest shells are often found aggregated in grape-like bunches
and are already attached.

2. The youngest observable stage consists of basal appendage and
living chamber.

3. The basal appendage reaches about half the size of the living
chamber and is stouter and more resistible than the latter. The relative size
and strength of the two parts suggests, not only the question after their
relative age, but also the possibility that the basal appendage was the
preceding one of the two. Though this problem can only be solved
conclusively by the finding of still younger shells, it may be permissible to
point out some facts which would seem to support the supposition of the
earlier appearance of the basal appendage. Its relatively great size and
thickness in the youngest stage have already been mentioned. But it is soon
outgrown by the living chamber, for while it begins with a length of .3 mm.
(cf. Pl. IV, fig. 4), it reaches only 4 mm. in the largest cup observed, which was
found in a detached state, and none were found in connection with the shell

broader than 2 mm. The living chamber, on the other hand, grew from a

g
length of .8 mm. to one of 14 cm. and perhaps still more. As it is obvious
that the basal appendage began relatively large but did in no way keep up in
growth with the living chamber, it is probable that it was an organ of
importance only in the youth of Conularia gracilis. Moreover, as it appears
to be in the later stages so strangely out of proportion to the size and
supposed weight of the animal and as it is absent in all known adults of the
various forms of Conularia, it may have been dropped entirely at adult
age. Perhaps it was the first hard-tegument appearing on the embryo, and
the suggestion of A. E. Verrill* that the appendage is “the initial secretion of

” seems to be not imappropriate.

the shell gland of the veliger-like young
It should, however, be remembered that the appendage also grows and does
not remain stationary as do the embryonic chambers of the Cephalopods, to
which one might feel inclined to compare it.

As the general trend of development is from sessile to slowly moving
and from these to faster moving animals, it seems reasonable to regard the
presence of the appendage in youth as a true palingenetic character indicating

the derivation of Conularia from sessile forms.

*American Journal of Science, Vol. II, July, 1896, p. 80.

718 Report oF THE STATE GEOLOGIST.

4. It becomes further evident from the study of the minute shells that
the latter were round and that the marginal grooves were only part of a
superficial layer. The fact that such multitudes of the youngest shells could
be so well preserved while the more advanced stages become rarer in propor-
tion to their size, as well as the excellent state of preservation of the former,
can not but suggest that the shells were relatively much stronger in the
younger stages than in the later ones. On the other hand, a comparison
between the young and old forms impresses upon the observer the greater
relative stoutness of the marginal grooves in the latter. They are for the
most part hardly noticeable in the infantile stage, and when the specimens
are flattened they have often no effect upon the outline which is then curved
(cf. Pl. IV, figs. 5, 10, 14, 17, 18, 21, 28, 32). It can, therefore, be said that
while the younger stages of growth had stouter walls and less prominent mar-
ginal grooves, with advancing age the walls of the faces became relatively thin-
ner and the walls of the marginal grooves stronger. This gives the impression
that there had been a tendency to make the shell lighter and at the same time
to preserve its strength; a tendency which would be only of advantage in
changing a sessile mode of life either to a creeping or swimming one. Thus
it seems that the well-known fact of the thinness of the shells of most species
of Conularia which suggest a swimming mode of life, and the observation of
the attachment of the rather stout shells of our species in its infantile and
adolescent stages, can be made to harmonize by assuming that Conularia
represents a group of animals which were in the process of adapting them-
selves from a sessile to an errant mode of life. It is probable that in most
forms, especially those of the Devonian and Carboniferous ages, the onto-
genetic course of development was materially shortened ; hence the absence
of such developmental stages as Conularia gracilis has furnished.

It has already been shown by the structure of the basal appendage
and the mode of occurrence of the growth stages possessing it, that these
youthful forms were also capable of some change in place of attachment.

The slight development of the surface sculpture in the young shells and
the preponderance of the transverse ribs over the longitudinal ones in some
of the best specimens (cf. Pl. IV, figs. 832 and 35) are perhaps also characters
of some phylogenetic significance.

Granted, then, that the described features of the young of Conularia
gracilis ave of a palingenetic character, it would follow that this Conwlaria
took its origin from animals with slender, conical, little sculptured,

chitinous shells, which were attached by basal, cup-like appendages.

RuEDEMANN—SEsSILE ConvULARIA,. 719

The marginal grooves and pyramidal shape would appear to be of secondary
acquisition.

Bearing in mind these supposed characters of the ancestors of Conularia,
the suggestion of A. E. Verrill in the above-mentioned paper that Conularia
represents a very primitive genus belonging to the Cephalopods appears quite
reasonable. The Pteropods, to which Conularia has been so long referred,
are claimed by zodlogists to be a very late class, while the Cephalopods are
recognized among the fossils of the Cambrian and were, probably, at the
beginning only sluggish or even sessile animals which acquired the power of
fast motion later. The chitinous material of the shell of Conu/aria seems to
the writer. to be no ground for objection, for there still exists to-day a group
of Cephalopods with chitinous shells, viz.: the Chondrophora of P. Fischer.
Further, the suggestion made in regard to other classes of shell-bearing
animals, that chitine was probably the original shell-material which has been
replaced later by other materiais, probably holds also true for the Cephalopods.
There are a few observations which point to this supposition. Hyatt* and
Holmt observe that the protoconch of Hndoceras (Nanno) belemn itiforme and
of other Vauti/oideu is represented by a cicatrix only and hence was fragile
and easily destructible. Hyatt concludes from this observation that the
protoconch of some Nautiloids was chitinous; others, as shown by Clarke,t
possessed already a calcified protoconch.

The occurrence of septa in certain species of Conularia,s though of no
great significance, indicates at least, that the animal advanced in the shell.
The Cephalopods did the same, but in a manner which proves their higher
development also in this regard.

If the genus Conularia indeed represents a group of transitional forms,
it would seem appropriate to recall the fact that progress from slower to
faster swimming was attained among certain Cephalopods (the LBelemnites) by
reducing and enclosing the shell, and to consider the possibility that the
Conularia did not become extinct, but taking part in the general progress of
the class, developed into Cephalopods with an internal shell and became thus
less hable to be preserved in a fossilized state.

Referring to this possibility, it should be borne in mind that the above-
mentioned Chondrophora, which are characterized by a chitinous gladius, have

not yet been linked phylogenetically to any group of the fossil Cephalopods,
a phytog : y grouy / }

* Genesis of the Arietidae, 1889.

+ Geologisk Férenings Férhandlinger, Vol. XVII, 1895.

~ American Geologist, Vol. XTV, October, 1894, p. 205, pl VI.

§ As many as three septa have been observed in the same specimen (cf. A. Ulrich, Palwozoische Versteinerungen aus Bolivien,
1892, p. 32)

720 Report oF THE SrarE GEOLOGIST.

while they appear at the same time (Lias), when Conu/aria makes its last
appearance in a single species,* after it had furnished only one other specimen

in the Trias.+

* Conularia cancellata, Argéliez, Middle Lias of the Dep. Aveyron. Ball. Soc Géol. France, 2 sér , Tome XIII, 1856, p. 187.
t Conularia triadica, Bittner. Hohe Wand bei Wiener Neustadt. Verhandlungen der K. K. Reiclsanstalt, 1878, p. 281, 1890.
p. 177.

Ea RUANADION OF PLATES.

46

Prate I.

Figure 1. Conularia gracilis, Hall, Utica slate, Dolgeville, N. Y., with attached young. a, wall
pressed out; 7, transverse striation of groove; c, apertural process of wall; s, sculpture of surface

discernible. x 2.

wo

FIGURE C. gracilis, with attached young. ss, fragments of sculptured wall. 2.

Figure 8. Young C. gracilis, with four distinct edges, attached to an older shell. 2.

he

FIGURE Detached specimen of (0. gracilis. s, surface film. x 2.

Group of very young specimens of Conularia cf. gracilis, Hall, attached toa shell

ot

FIGURE
fragment. 2.

Fieurer 6. (. gracilis. Fragment of the wall. x 2.

PLATE 1

CONULARIA.

ce ae A ee

°

Puate II,

Fieure 1. @. gracilis on Trochonema cf. ammonius, Hall, Natural size,

Ficure 2. Sulcus at the edge of C. gracilis, exterior view. a, surface film; 6, second film
c, filling prism; /, side walls of groove. x4. ;

Figure 3. The same, interior view. x4.

Frevre 4. The same, transverse section. x4. °

Fieure 5. C. gracilis. Natural size. :

Figure 6, Enlarged sculpture. x 13.

Fieurs 7. Conularia cf. gracilis, Hall, (Sphenothallus angustifolius, Hall). s, sculpture of surface

discernible. Natural size.

PLATE {1

UC

CONULARIA,

;

> es "

yee wi
Lang

“ ~
i t=
al eas
‘
"3
- . ~~
“
ta '
f <=
¢
‘
i - a
eyo
7
!
* f) ®
'
j
1
4 ‘ . *
i mts
’
‘ +3
ag
kaa
¥
(;
i
7
a “4
i
dh
6) 78
‘y ' é
+
‘
t 4
TU
i
= ed 2
a) * - e
oe ae
2 es '
fi i
nel
te ‘
5 { r i
,
,
Nn
F
=
S
' 6
ima? "4 a:
a, {
i

”

'-
.
At
‘
o
‘
~
4

PuLatTe III.

Conularia gracilis, Hall. Utica slate, Dolgeville, N. Y.

Fieure 1. Dorsal view of basal appendage. Enlargement of the appendage of the specimen
reproduced in Plate II, Figure 1. » 10.

Ficure 2. Vertical section through appendage. Whole specimen as found. 10.

Figure 3. Nearly vertical section. «, basal ring of exterior bell, seen from inside; b, dorsal part
of bell; c, interior cup. »x 10.

FieurE 4. Detached specimen of Conularia gracilis, bearing the appendage reproduced by
Figure 3. Natural size.

Freure 5. Underside of appendage. a, base of exterior bell; 6, base of interior cup. X10.

Ficure 6. Ventral view of appendage, only the bases of exterior bell (a) and interior cup (0)
being preserved. x10.

Ficure 7. Ventral view of appendage. a, base of exterior bell; 6, base of interior cup. x 10.

FieurE 8. Ventral view of appendage, showing the radial furrows of the base of the exterior bell
and the concentric structure of the latter. x 10.

Figure 9. Lateral view of basal appendage. a, dome of bell; 6, basal ring of bell; c, impression
of base of bell; ¢, impression of basal skin; ¢, node in centre, cast of central cup. x 10.

Figure 10. Interior view of bell from ventral side, shows wrinkled dome of bell and subqua-
drangular entrance of pyramid of Qonularia. 10.

FiGuRE 11. Counterpart of the preceding. Shows the apex of the pyramid. x10.

FicuRE 12. Dorsal view of appendage. Dome of bell broken away. x 10.

FreurE 13. Ventral view of appendage. Shows radial striation of base of bell. x 10.

Freure 14. Conularia gracilis, Hall, attached to a fragment of Stictoporella. Natural size.

FrcurE 15. The same. Basal appendage as found originally. x8.

FieurE 16. The same. Matrix removed by acetic and hydrofluoric acids. a, interior bell;
}, impression of connecting basal skin; c, impression of central cup. x8.

Figure 17. Ventral view of appendage. Exterior bell seen in section. Exhibits apex of
pyramid. x6.

Figure 18. Ventral view of appendage. a, base of bell; >, base of central cup. x 10.

Figure 19. Impression of basal appendage. Junction of two marginal grooves of pyramid
preserved. x 10.

Figure 20. Transversal section through appendage. Shows the four marginal grooves of the
shell of Conularia in section. > 10.

Figure 21. Diagrammatic section through basal appendage. The dotted part is a section
through the basal appendage in the state of compression, the striated through the same in the state of

attachment. » 10.

PLATE IIf

CONULARIA

se ee ey ee eee

ian
de

=e eee

*

Pruate IV.

Conularia gracilis, Hall, Utica slate, Dolgeville, N. Y.

FIGURE 1.
FIGuRE 2.

FIGURE 3.

Group of young. Natural size.
Group of young. Natural size.

Young attached to a small projection. Natural size.

Ficures 4 to 35. Various growth stages. x 4.

FIGURE 36.

or
‘

FIGuRE 37.
FIGURE 88.
FIGURE 39.

FIGuRE 40.

Uncompressed specimen. 4.

Slightly compressed specimen, 4.
Uncompressed specimen, x 4.

Specimen terminated by septum. Natural size.

Type of Sphenothallus angustifolius, Hall, Canajoharie, N. Y. Natural size. a, young

specimens attached; }, natural section, showing the composition of the pyramid of four faces.

728

PLATE Ly

RH =

CONULARIA

NOTES ON SOME CRUSTACEANS FROM THE CHEMUNG
GROUP OF NEW YORK.

By JOHN M. CLARKE.

%,

‘Notes on Some Crustaceans from the Chemung Group of
New York.

By Joun M. Crarkr.

I. A Singularly Ornamented Phyllocarid Genus, Pephricaris.

By the courtesy of Professor A. R. Crandall, of Alfred university,
Alfred, N. Y., and the kindness of Mr. Charles Butts, of the same place, I
have been permitted to study specimens of a new crustacean allied to Avhi-
nocaris, but noteworthy for the extravagant nature of its armature. Of these
specimens, two in number, the more complete belongs to the museum of
Alfred university and is a sculpture-cast of essentially the entire test, the
valves of the carapace being expanded without distortion and the abdominal
seoments showing, in part, in the posterior hiatus of the carapace valves and
thence normally protruding behind. The second specimen, the property
of Mr. Butts, is only the echinate margin of one carapace valve.

The general aspect of the carapace is not unlike that of some species of
Echinocaris, yet it is devoid of the curved sigmoid carina which characterizes
typical species of that genus.

The carapace valves are broad, their margins curving rapidly outward
for about one-half of their length, slowly recurv-
ing near the middle and thence more rapidly
receding to the posterior extremity. The expanded
valves lie with a moderately broad anterior or
rostral cleft, but there is no evidence of a separate
rostral plate. They are in contact just back of the
apex of this cleft, but for only a short distance, as

the underlying abdominal segments are partly

exposed, a fact which may be due either to this

being the normal attitude of the valves, or to casual

FIGURE 1.

separation of them, or again to a breaking of the Pephricaris horripilata, Chemung
sandstone, Alfred, N. Y.

edges of the cast which is not altogether clear at this
place. The surface of each valve is divided into two convexities by an oblique
depression beginning at the dorsal edge just back of the middle and extend.

ing backward with gentle obliquity. This groove does not reach the margin
731

7392 Report oF THE SratE GEOLOGIST.

of the valve. The anterior convexity is much the larger. Usually, in Hehi-

nocaris, there is a number of paired nodes and tubercles grouped about the
cephalic extremity of the carapace, but in this fossil there is only a single
pair, represented by two deep pits situated close upon the hinge and at the
apex of the rostral cleft. It is possible that these are remains of ocular
nodes, but their depth suggests the probability of their having been basal
attachments of the larger legs. Behind these nodes begins an oblique and
strong ridge, thickest and most elevated at the hinge, where the anterior
edges of the ridges on the two valves meet. This ridge departs backward
into the median groove, passes down its anterior slope, then, with a slight
change of angle, along the groove and rises slightly on its opposite slope,
terminating with the groove itself. The margin of the carapace is some-
what thickened and elevated.

Nowhere in Achinocaris do we find a carapace structure like this, even
among the species of the Chemung group. The lateral curved carina is one
of the constant characters of the genus and may even be duplicate in later
species. The median sinus exists there, normally, only as a depression
between nodes, and no species is so free of cephalic nodes as this.

As to the abdominal segments, we find that three, and a portion of a
fourth, protrude beyond the carapace ; between the carapace-valves we make

out traces of two or three others, estimating the entire
number at seven. The posterior segments are unusually
short and have short spinules at their post-lateral extremi-
ties ; there may, also, have been such spinules elsewhere along
the posterior edge as in /ichinocaris, but such are not seen.
The caudal plate is short and triangular, with a short telson
and two long curved cercopods.

FIGURE 2.

Pophicuns home: The fossil bears a striking ornamentation or armature.

eee ee of The entire outer margins of the carapace valves carry a

single row of broad, strong, erect and slightly recurving
spines. These are shortest at their commencement on the anterior margin,
gradually increase in size posteriorly, their greatest length being reached
on the post-lateral curve, and thence to the posterior angle of the
carapace they become shorter. The maximum length attained by these
spines is not less than one-half of the greatest diameter of a carapace valve.
That these processes are spinous extensions of the chitinous test substance,
and not bundles of setz, or of other nature, is shown by the aspect of the

imprints they have left in the matrix, these being sharply defined |

CLARKE—CRUSTACEANS FROM THE CHEMUNG GRoUP. 733

and clean-edged throughout their extent; and again by the presence of similar
but straighter and more slender spines upon the final segment of the abdomen.

Of the latter, two pairs are visible, the penultimate pairs appearing to be
somewhat longer than the ultimate; there are traces also of a similar pair on
the antepenultimate segment.

This description presents all the known characters of this peculiar
crustacean. Its essential structure is nearest to Hchinocaris and yet not in
harmony with that genus, and its extravagant decoration emphasizes that
‘generic difference. For this reason the generic term Pephricaris is adopted
for the fossil, and the species may be known as Pephricar’s horripilata.

Both specimens of the species were found in loose blocks of compact
Chemung sandstone at Alfred, N. Y. Neither shows associated fossils.

II. The Chemung Trilobite, Bronteus senescens, Clarke.

In the Report of the New York State Geologist for 1888, the writer
described the trilobite above named.* The single specimen upon which the
description then published was based, was but a very imperfect fragment of
a pygidium and the only justification for drawing attention to the fossil was
the extreme rarity of all trilobites in the Chemung faunas. At the date of
that writing the presence in the Chemung of the species Phacops ana, Green,
common in the Hamilton rocks beneath, and not of infrequent occurrence in
the Ithaca fauna immediately below the Chemung formation, was suspected,
and had been announced. Later evidence has not confirmed this statement,
and we know to-day only two described species of trilobites from this fauna ;
the Cyphaspis levis, Hall (sp.), the original and only known specimen being
a cephalon, and Brontews senescens. The presence of the genus Homalonotus
is shown by a fragment from the higher beds in Alleghany county. Since
the description of Bronteus senescens, founded on a specimen from the lower
Chemung strata in the town of Prattsburgh, Steuben county, additional
material has been obtained which sets forth the characters of the species in its
entirety and also shows that from the fragment previously figured and the
restored outline at that time given to the pygidium, it might prove difficult to
recognize the species when at its best. A restatement of the characters of the
fossil drawn from our amplified knowledge of it, will therefore serve to clearly

define the value of this species.

* The Genus Bronteus in the Chemung Rocks of New York, op. cif., Figure 1 ; also published in Forty-secund Annual Report
Trustees State Museum, pp 403-405.

734 Report oF THE STatTE GEOLOGIST.

Soon after the publication of, the article above cited, the writer located
the horizon at which this fossil occurs, on Bardeen’s farm in the northern
part of the town of Prattsburgh, finding here several nearly entire pygidia.
This horizon is well characterized by the constant association of this trilobite
with the crinoid Arthracantha depressa; a species recently described by
Wachsmuth and Springer from specimens collected at this locality where its
spinous plates are very common. It is the zone of /ehynchonella (Pugnaa)
pugnus, Sow., and is an eastward extension of this zone from its somewhat
more prolific manifestation at High Point, in the town of Naples. More’
recently two essentially entire specimens of the trilobite have been obtained
from higher strata of the Chemung group, near Avoca, Steuben county,
through the agency of Mr. Clifton J. Sarle, both excellently preserved though
lacking a few details, but presenting us with a really striking exemplh-
fication of the late continuance of this genus.

Figures of these specimens are here given and the description of the

characters of the species is as follows:

FIGURES 3 and 4. Bronteus senescens ; two nearly entire individuals from the Chemung group,

near Avoca, N. Y.

GeENERAL Proportions. The outline of both of these extended
individuals is quite regularly ovo-elliptical, the shorter curve being at the
posterior extremity. In length the larger measures 54 mm., the smaller, 46
mm., while the greatest width of the animal is about one-half this dimension
in both cases. The specimens have been subjected to slight, if any, vertical
compression though the heads are somewhat askew; the lines of the margin

may, therefore, be regarded as normal.

CLARKE—CRUSYACEANS FROM THE CHEMUNG GRouP. 735

CrpHaton. The head is short and subsemilunar in outline, the posterior
margin being quite direct. Its length is shghtly more than one-half its width.
The genal angles are somewhat produced into short and broad spines. The
margin is elevated, while the border of the head is broadly concave, rising on
its proximal limb to a genal ridge. The eyes are small, well back on the
cheeks and moderately elevated, the surface between the palpebrum and the
dorsal furrows being notably convex. The facial sutures are normal.
The glabella is elongate and clavate, its width at the anterior extremity
where it reaches but does not overhang the margin, being twice that just in
front of the occipital ring. In contour it is depressed convex, though its
elevated median portion attains greater elevation than any other part of the
cephalon. The dorsal furrows are deep and narrow; starting from the
posterior margin they approach each other rather abruptly ; the curve changes
at the level of the posterior part of the eyes and thence forward the furrows
diverge outward rather gradually, broadly recurving near the anterior margin.
The lateral furrows are short but distinct, the first and third pairs being
most clearly defined, a median pair making but a gentle depression upon the
surface, while the occipital groove is broad and shallow.

The occipital ring is likewise broad and distinct, but its prolongation to
the cheeks is narrower and much more faint.

. In one of the specimens the removal of the part of the glabella has
exposed a portion of an elongate Aypostome with an oval central depression,
surrounded by a narrow regular groove and bordered by a narrow flattened
margin.

THorax with the normal number of ten segments. The axis is very broad,
having fully one-third the entire width of the thorax, and its margins curve
outward, approaching each other posteriorly. On the axis the segments are
moderately broad and flat, distinctly elevated along the median line with
general longitudinal depressions on the lateral slopes and a slight anterior
bend at the sides. On the pleurv, the segments are narrow and soon become
free of each other, tapering rapidly to slender, recurved, acute extremities.

Pyemrum semielliptical, flabelliform; length and width about equal.
Axis very short, extending for not more than one-fifth or one-sixth of the
plate; triangular, elevated medially and with an obscure central lobe and
depressed lateral slopes. The pleure are broad, flat, separated by sharply
defined flat grooves. They broaden rapidly outward and finally become
merged into the grooves near the periphery of the plate, so that the margin of

the latter is smooth. These ribs are fifteen in number; the median rib being

736 Report oF THE STATE GEOLOGIST.

somewhat broader than the rest and, in the larger specimen, showing a
tendency to division along its distal portion. The margin of the pygidium is
without evidence of spines. In general contour this plate is broadly depressed
within the slightly elevated periphery, convex over the central region and
again sharply depressed about the axis.

Ornamentation. The entire test is pretty uniformly pustulose, the
pustules varying somewhat in size and being coarsest on the glabella and the
ribs of the pygidium. About the enfolded margins of the cephalon and
pygidium the surface is marked by the usual incised inosculating lines.

Oxservations. This species is noteworthy not alone for the rarity of all
trilobites at this horizon. It is, in all probability, the latest representative
of the genus, making its appearance in this later division of Devonian time,
subsequent to the first intrusion of Spirifer disjunctus and long after the
only observed occurrence in this country of Clymenia. It appertains to a
fauna which, considered in its local relations and in correlation with faunas of
other countries, characterizes the final stages of the Devonian, and in these
we have no other record of the occurrence of Gronteus. In this late survivor
of the genus, therefore, we may expect to find structural traits indicative of,
or in harmony with its late appearance. We observe that between the earlier
(upper Silurian and early Devonian) and the later Devonian representatives of
this genus there are contrasts in the form of the glabella, the outline of the
pygidium and the nature of its ribs. Thus, the glabella (or we should rather
say the cranidium, as the distinction depends on the varying distance between
the facial sutures) is very wide anteriorly, the dorsal furrows being highly
concave within the ocular nodes (compare 4. palifer, Beyr., Lower Devonian,
Zittel’s figure, Grundzige der Palzontologie, p. 473, fig. 1,279a; Katzer’s
figure, Geologie von Boéhmen, p. 1,023, fig. 498-4; L. campanifer, Beyr.,
lower Devonian, Beyrich’s figure, Einige béhmische Trilobiten, Plate, fig. 6;
L. Partschi, Barr., wpper Silurian, Katzer’s copy of Barrande’s figure, op. cit.
p. 937, fig. 377-2; B. viator, Barr, lower Devonian, Novak’s figure in
Katzer, op. cit., p. 1,036, tig. 548-1; B.acamas, Hall, Niagara group, Twentieth
Annual Report New York State Cab. of Natural History, Pl. I], fig. 19;
BL. lunatus, Billings, Trenton limestone, Geology of Canada, p. 188, fig. 187,
and Clarke’s figure, Geological Survey of Minnesota, Vol. III, Part 2, p. 725,
fig. 43). In all of these and numerous other recorded examples the feature
referred to is strongly manifested. If on the other hand, we turn to species
of the middle Devonian, the narrowing of the glabella and the interval

between the facial sutures becomes evident (see B. jflabellifer, Goldtuss,

‘
2

CLARKE—CRUSTACEANS FROM THE CHEMUNG GRoUP. 737

System. Uebersicht, Pl. VI, fig. 8; BL. meridionalis, Trom. and Grasset,
Barrois’s figure, Cale. & Polypiers de Cabriéves, Plate I, figure 2a.
DB. thysanopeltis, var. Waldschmidt, v. Koenen, Waldschmidt’s figure, Zeitschr,
d. d. Geol. Gesellsch., Vol. XX XVII, Pl. XX XVIII, fig. 2; B. senescens, ete.,
etc.). This feature appears to be one which, irrespective of other variations
in structure, has gradually passed through the change noted, and it 1s,
naturally, to be observed that lower Devonian faunas embrace species, some
with the wide, some with narrower glabella, while thereafter, the earlier
type of glabella has disappeared.

With reference to the characters of the pygidium in this genus it may be
remarked that the only really useful, tenable subdivision of the group is
founded upon the presence of spinules upon the pygidial margin. This is
Thyanopeltis, one of the names introduced by Corda and designed by its
author to include species of this character; it has proven to possess a definite
stratigraphic value. In matter of outline there is considerable variation, from
the subsemicircular shape in the earliest species like 2. /unatus, Bill., of the
Trenton, 2. daticauda, Wahlenberg, of the lower Silurian of Sweden, and L.

hibernicus, Portlock, of the Caradoc, to the elongate-elliptical curve presented

by the species of the Devonian. In this feature B. senescens is extreme,

surpassing the elongate, narrowing tail-plate of L. Avelcensis, Girich, of the

-lower upper Devonian (Cuboides horizon) of Poland. Corda (Prodrom einer

Monographie der béhm. Trilobiten, pp. 58, 59, 1847), attempted a further
division of the genus on the basis of the simplicity or duplication of the
median rib of the pygidium, proposing for such species as show a bifurcation,
the name Dicranactis, and for those in which it is simple, Ho/omeris. It has
long been evident, and is shown in the species in hand, that the duplicatioa
of this rib is of such minor significance that it can be regarded only as an
individual character and we can not safely infer values from this trait.

Barrande observed (Systeme Silurien, Vol. I, p. 840) that a division of
the species of Drontews might be founded upon the number of ribs on the
pygidium, which are either six, seven or eight on either side of the median
rib. By far the greater number of species possess seven ribs, while six such
ribs are present only in the earliest species, ¢. ¢., Bb. /unatus, B. hibernicus,
B. laticauda. Herein LB. senescens, having seven ribs, perpetuates the struc-
ture of the normal representatives of the genus.

The definite time value of the subgenus 7/ysunope/tis has been set forth
by Barrois, Kayser, Frech and other writers. The only representative of this

division yet known in American faunas is the species 2. tu//ins, from the

738 Report oF THE Strate GEoLoGIstT.

Tully limestone (Cuboides horizon) of New York. Though the group is
well represented in lower Deyoman horizons, there is no record of its per-
durance beyond the Cuboides horizon, and we notice that in this late represen-
tative of Thysanopetis the marginal spies are minute and hair-like. © Within
the limitations of this group we find the glabella passing through variations
in dimensions quite similar to those which characterize the genus as a whole.

Bronteus senescens is devoid of marginal spines and reproduces the char:
acters of the normal middle Devonian type. We look upon this species,

therefore, as distinctly progressed in the character of its glabella and pygi-

dium and as having escaped entanglement with the early Devonian divergence

into Thysanopetis; a survival, with appropriate time modifications, of the

proper expression otf the venus.

PRELIMINARY

GEOLOGIC MAP

°o

ALBANY COUNTY
N

W YORK.

ALL State Geologist
N.A Darton)

One Inch - One Mile

a j

WA ay ena

em tac
"7 os

sia
t 2%

ei, /
2 4—
¥

aK)

: ¥

‘ \ | AA 1 ‘| ) "
NALD Lys \ y
Way

HA (
J Explanation of Colors
ONEONTA FORMATION
Ried Shalos and Flags
HAMILTON FLAGS ano SHALES

HAMILTON SHALES

ONONDAGA LIMESTONE

DEVONIAN

ESOPUS SHALES
(Candi Galli)
ORISKANY SANDSTONE

Becraft Limestone

Shaly Limestone

QuaRRIES Pent amerus Limestone

Nole The brown lines are Contour lines which FLAG STONE
South an ROAD METAL
feet in the Northwestern corner of the County. BUILDING STONE
MOULDING SAND WATER-LIME
BRICK CLAY

Tentaculite Limestone

SILURIAN
HELDERBERG LIMESTONES

TT TST VBL | Naga

HUDSON RIVER FORMATION
Shales an¢ Sandstones

ro

TL

\S