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Published monthly by the wr

‘s a) ; t ot “Th a we te ' ton Foal

| SN ee

New York State Education Department

BULLETIN 303 FEBRUARY 1907

>

New York State Museum 1

ey 7
Teen, OG

Joun M. Criarxke, Director

Bulletin 106

GEOLOGY Il

C”ACIAL WATERS IN THE LAKE ERIE BASIN

BY

H. L. FAIRCHILD

PAGE PAGE
Wiairodtuetion ... Jeska. 5 | Glacial drainage channels..... mS
URAL LEO LE. il aia ayaled Git St: 6 |) ILoczlvelleierall leikesaceepeoeose Se
Esch VIS ne LN od a5 Sebeig. soe « 7 i iGreater elacaliflakesty ses jae AI
Geography. Topography..... 8 | Shore lines of the greater lakes 44
Outline of glacial history..... 9 | Deltas and lake plains........ 79
Ice margins: moraines........ Histol Ww ulnaclex: 2 21.5% § Sis hy aes See ee 85
eon I : y , _
ALBANY ;
NEW YORK STATE EDUCATION DEPARTMENT JUN t
1907 \8A2O<

M146m-Ja6-1000 Ts = ‘ Price 35 “eanttes<

1913
1917
1908
1914
Igi2
1918
1gI0
IQrs
IQII
1909
1916

STATE OF NEW YORK | Bae
EDUCATION DEPARTMENT

Regents of the University

With years when terms expire

Tiana Reip M.A. LL.D. Chancellor Mee : New York .

Sr CLAir McKetway M.A. LL.D. Vice Chancellor Brooklyn -
DANIEL Beach Ph.D. LL.D... .° 2. ee
Piiny T. SEXToN LL.B. LL.D. . .. .. = Paliapes

T. Guitrorp Smira M.A. C.E! LL.D.) 2” 2a
Witiiam NottincHaM M.A. Ph.D. LL.D. . . Syracuse
CuHar Les A. GARDINER Ph.D. L.H.D. LL.D. D.C.L. New York
ALBERT VANDER VEER M.D. M.A. Ph.D. LL.D. Albany
Epwarp LauTtersach M.A.LL.D. . + . . New Yorks:
EvuceEneE A. Puitpin LL.B. LL.D. . 2 ee NG waliorls

Lucian L. SHEDDEN LL.B. re raises 5 8 SKS eo ner

Commissioner of Education

ANDREW S. Draper LL.B. LL.D.

Assistant Commissioners

Howarp J. Rocers M.A. LL.D. Furst Assistant
Epwarp J. Goopwin Lit.D. L.H.D. Second Asststant
Aucustus S. Downine M.A. Pd.D. LL.D. Third Assistant

Secretary to the Commissioner

Harvtan H. Horner B.A.

Director of State Library
Epwin H. ANpERSoN M.A.

Director of Science and State Museum

Joun M. Crarxke Ph.D. LL.D.

Chiefs of Divisions

Accounts, W1LL1AM Mason
Attendance, James D. SuLLIVAN
Educational Extension, WILLIAM R. Eastman M.A. B. L.S,
Examinations, CHARLES F. WHEELOcK B.S. LL.D.
Inspections, FRANK H. Woop M.A.
Law, Tuomas E. FINEGAN M.A.
School Libraries, CHARLES E. Fitcnu L.H.D.
Statistics, Hiram C. CasE .
Visual Instruction, DELANcEy M. ELtis

New York State Education Department
Science Division, January 13, 1906

Hon. Andrew S. Draper LL.D.
Commissioner of Education
My bDeEAR sir: I beg to communicate herewith for publication as
a bulletin of the State Museum the manuscript of a paper entitled
Glacial Waters 1n the Lake Erie Basin by Prof. H. L. Fairchild, ex-
pert assistant on the geological survey.
Very respectfully yours
Joun M. CLarK4E
Dvwrector

Approved jor publication, January 15, 1906

Ee es

Commissioner of Education

7h

ie

MU,

New York State Education Department

: New York State Museum

Joun M. Crarxke Director

Bulletin 106

GEOLOGY Il

' GLACIAL WATERS IN THE LAKE ERIE BASIN

BY

H. L. FAIRCHILD

INTRODUCTION

In former papers on the glacial waters of central western New
York the writer has described mainly the phenomena in the Ontario
basin. The present paper is the result of study distributed through
several years in the Erie drainage area, and it discusses glacial effects
which antedate those in the Ontario basin. The writing is intended
as the first of a series describing the effects of glacial waters in New
York State and treats of the westernmost geographic area, where the
phenomena are of earlier date than those eastward, as the greater
glacial lakes invaded the territory from the west.

There has also been a personal reason for delay in this writing.
The studies of Mr Frank Leverett on the Pleistocene geology of
Ohio and the Erie basin led him in 1893 into New York as far as the
Genesee river. The results of this earlier work have been awaiting
publication and the writer has delayed the completion of his own
study in the Erie basin in order to give precedence to that
which now has been published as Monograph XLI of the
United States Geological Survey. The present writing covers
ground traversed in Leverett’s report and deals with the same
phenomena; but the manner of treatment is somewhat different,
the description is more detailed and in some points the interpre- -
tation or explanation of the phenomena is not the same.

The writer has ventured to differ from Leverett’s description or
interpretation only where the facts seemed imperative, and his best

6 NEW YORK STATE MUSEUM

apology is the statement that much greater opportunity for study
of the region has given superior advantage. The greater part of
the field work was done before Leverett’s descriptions and maps
appeared, but these have been suggestive and helpful and have
caused reexamination of some districts. Inthe belt of stream chan-
nels and lake beaches nearly every highway has been traveled, many
in both directions, and many features have been examined from
different viewpoints. Some districts have been visited several
times, yet there is a mass of interesting detail almost untouched,
which possibly has entailed some minor errors in fact or interpreta-
tion in the paper. A resident in almost any portion of the area
can find, after training his eye and mind to see and understand
them, many other interesting features resulting from the work of
the glacier or the glacial waters. The writer has satisfaction 1n the
thought that many people living in the area described will find a new
source of pleasure in having their attention directed to these ro-
mantic geologic phenomena.

LITERATURE

Very little systematic work on the phenomena of glacial waters in
the New York portion of Lake Erie basin has been done except by
Mr Frank Leverett, although the beaches have long been recog-
nized. In Leverett’s Monograph XLI he gives on pages 28-49 a
full list of works which contain any reference to the glacial geology
of the region. It is not desirable to repeat that list here, but a few
writings which have more immediate reference to the New York
area are noted below.

. Bishop, Irving P. Geology of Erie County, New York. N. Y. State Geol.

i5th An. Rep’t. 1897. 1:17-18, 305-92.

Carll, J. F. A Discussion of the Preglacial and Postglacial Drainage in

Northwestern Pennsylvania and Southwestern New York. 2d Geol.

pur. Pa. Rept TIL. 31882.

Chamberlin, T. C. Preliminary Report on the Terminal Moraine of the
Second Glacial Epoch. U.S. Geol. Sur. 3d An. Rep’t. 1883. p.291—

402.

Claypole, E. W. Preglacial Topography of the Great Lakes. Can. Nat.
1878. 8:187—206.

Origins of the Basins of Lake Erie and Lake Ontario. Am. Ass’n Adv.
Sci. Proc. 30:147-59. Also in Can. Nat. n.s. 1881. 9:213—27.

Edson, Obed. The Glacial Period in the Chautauqua Lake Region. 1892.

TiO)

Fairchild, H. L. Glacial Lakes of Western New York. Geol. Soc. Am. Bul.
1895. 6:353-74.

Lake Warren Shorelines in Western New York and the Geneva Beach.

Geol. Soc. Am. Bul. 1897. 8:269-86.

Glacial Genesee Lakes. Geol. Soc. Am. Bul. 1896. 7:423-52.

—— Glacial Waters in the Finger Lakes Region of New York. Geol. Soc.
Am. Bul. 1899. 10:27-68.

Glacial Lakes Newberry, Warren and Dana in Central New York. Am.

Jour. Sci. 1899. 7:249-63.

GLACIAL WATERS IN THE LAKE ERIE. BASIN 7k

—— Latest and Lowest Pre-Iroquois Channels pewices Syracuse and Rome.
Neve Stace Geol, 21st An. Rept. 1903. p.32—47.

Summary of Work in the Erie Basin, with ‘Map of Lake Warren. N.Y.
Suate Geol. 22d An. (Rept. 1904. p: rr.

Gilbert, G. K. History of Niagara River. N. Y. State Reservation at
Niagara. 6th Rep’t. 1890. p.61—84.

Recent Earth-movement in the Great Lakes Region. U.S. Geol. Sur.
r8th An. Rep’t. 1808. pt 2. p.601—47.

Hall, James. Geology of New York: Report on Fourth District. 1843.
675 Pp.

Leverett, Frank. Correlation of New York Moraines with Raised Beaches of
Walkesime: ata our, Sei, ser. -3 1895. 50 :1—20.

Correlation of Moraines with Beaches on the Border of Lake Erie. Am.

Geol. 1898. 21:195-99.

Glacial Formations and Drainage Features of the Erie and Ohio Basins.
U.S. Geol. Sur. Monogr. XLI. 1902. 802 p.

Newberry, J.S. Onthe ona and Drainage of the Basins of the Great Lakes.
mimes hde soc. Proc. |) 1883. 20:91-95

Spencer, J.W. A Review of the History of the Great Lakes. Am. Geol. 1894.
14:289—301.

Tarr, R. S. Geology of the Chautauqua Grape Belt. Cornell Univ. Agric.
Exp. Sta. Bul. tog. 1896. p.g1—122.

Taylor, F. B. Correlation of Erie-Huron Beaches with Outlets and Moraines
in Southern Michigan. Geol. Soc. Am. Bul. 1897. 8:31-58.

The Great Ice Dams of Lakes Maumee, Whittlesey and Warren.
Am.Geol. 1899. 24:6—38.

Upham, Warren. Origin and Age of the Laurentian Lakes and of Niagara
Falls. Am. Geol. 1896. 18:169-77.

AREA, MAPS

The area described in this paper may be defined briefly as that
part of New York State which drains into Lake Erie; but the his-
tory of the glacial waters involves territory far east of the present
Erie drainage, as the valleys of Oatka, Genesee, Hemlock and
Honeoye were forced to send their overflow westward into Lake
Warren for a time during the later stages of our history.

The principal phenomena herein described lie in a belt parallel
to the present Erie shore and having a direction nearly northeast
and southwest [see pl. 1]. From the Pennsylvania state line to the
valley of Cattaraugus creek the belt is only 5 to 10 miles wide, and
‘from the Cattaraugus eastward the phenomena are not spread over
a much wider belt until near the Tonawanda valley. The distance
covered by the belt in direct course from State Line to Indian Falls
is about go miles.

The territory is included in the counties of Chautauqua, Cattarau-
gus, Erie, Wyoming and Genesee. In plates 1-6 the reader will have
before him the following sheets of the New York topographic map:
Westfield, Dunkirk, Cherry Creek, Silver Creek, Buffalo, Depew,
Attica, Batavia and Caledonia.

8 NEW YORK STATE MUSEUM

GEOGRAPHY. TOPOGRAPHY

The relation of the geographic elements in horizontal plane is
shown in the maps [pl. 1-6]. The vertical relation or relief is indi-
cated on the maps by the contour lines which give altitude in feet
above ocean level, and are drawn with a vertical spacing of 20 feet.

As a broad statement it may be said that the slope of the land sur-
face is toward Lake Erie. This is strictly true for the western part of
the area, but the eastern part inclines more to the northward, or
toward the Ontario basin. The slope is not a steady or uniform
inclination, as a large part of the fall is concentrated in a rela-
tively narrow belt, which is shown by the contoured maps. It is
along this steepest slope that the greater number of drainage chan-
nels occur.

The Cattaraugus valley is the only broad embayment which
breaks the continuity of the Erie slopes. South of the Cattarau-
gus the slope is not cut by any large preglacial valleys, but the
surface north of Cattaraugus is more dissected.

From State Line to the Cattaraugus valley the divide or water- .

parting between Lake Erie and the Allegany river drainage lies only
some 5 to 10 miles from the lake. The altitude of the divide is
over 1300 feet, while the lake surface is 572 feet. It is therefore
apparent that the land slope in this section is very steep, falling in
5 to 10 miles about 700 feet from the lowest passes or cols to the
lake, and from the hilltops falling about goo or tooo feet. This
fact of the steep slope facing lakeward is of special importance to
the clear comprehension of the glacial lake history. For more

particular description it will be necessary to discuss the area by sec- ©

tions.

From State Line to beyond Fredonia about one half the total fall
from the divide to the lake, or 400 to 500 feet, is found in about
1 mile of horizontal distance. This steeper slope forms the con-
spicuous high ground which bounds the view when looking landward
from the highways or the railroads. Just below the steepest slopes
lie the. shore lines of the ancient glacial lakes. From these old
beaches to the present lake the land has a gentle slope, being the
silted and leveled floor of those extinct lakes.

The Cattaraugus valley carries the divide far inland (eastward),
the farthest points being some 40 miles from Lake Erie. The old
beaches and glacial stream channels, however, curve up the valley
only as far as Gowanda.

From the Cattaraugus embayment to Hamburg the topographic
features are quite similar to those west of the valley. Beyond

— oe

GLACIAL WATERS IN THE LAKE ERIE BASIN 9

Hamburg, north and east, the land surface is more dissected by
streams and the general slope is more gradual. In consequence
of these characters the glacial stream and lake phenomena are
distributed over a wider belt and more irregularly.

With reference to both ancient and modern drainage there are
two sets of baselevels. The lowest is the present water surface
of Lake Erie, taken as 572 feet over ocean. The other baselevel
is the series of ancient and higher waterlevels of the great glacial
lakes Whittlesey and Warren. These old high-level beaches are
spread through a vertical space of about 70 feet, and lie just below
the foot of the steepest land slope.

The ancient shore lines are no longer horizontal, but have suf-
fered along with the land surface on which they lie a tilting or
differential uplift, so that they now rise toward the northeast at
the rate of nearly 2 feet a mile [see p. 77].

OUTLINE OF GLACIAL HISTORY: THEORETIC PROBLEM

It will help the reader to a clear mental grasp of the subject
if the broad features in the topography and the main events in the
geologic story can be clearly appreciated apart from details.

There are four distinct elements in this study. (1) The general
topography or the broader configuration of the land surface.
(2) The location and trend of the front of the glacier, which is the
variable factor. (3) The flow of the escaping waters, or the stream
phenomena, which changed along with (2). (4) The position
and the effects of the lake waters which followed the retreating
ice front. We will discuss these briefly in order.

(1) The general topography has already been described as a
broad valley or basin extending northeast by southwest. The
present Lake Erie has no part nor significance in this history, it
being only the successor of the ancient glacial lakes, and giving
its name to the basin, and marking the lowest part. The Lake
Erie basin should be recognized as continuing northeastward
beyond the lake, and as blending with the Ontario basin. The
southern slope of this general basin, facing northwest, and extend-
ing from the Pennsylvania boundary northeastward to Batavia,
is the stage on which our glacial drama was enacted.

(2) The geologic events which we are studying belong to the time
when the last ice sheet of the glacial period was disappearing from
the region. At an earlier time, when the great ice body was at its
maximum, it had covered, practically, all of New York State, and
the movement of the ice mass had been toward the southwest,

Io NEW YORK STATE MUSEUM

following the axis of the Erie basin. But at the time we are con-
_ sidering the ice sheet had long passed its maximum stage, and the
front had receded, due to the excess of melting at the margin over
the supply by flow from the northward. There now lingered over
the Erie basin a great mass or lobe of the continental glacier which,
since it was no longer subject to great pressure or push from the ice
mass on the north, was reposing in the basin as a comparatively
stagnant mass. It was not a rigid, inflexible body, like a small
block of ice in the summer sunshine, but its great bulk and weight
gave it a practical plasticity and a slow spreading movement, like a
block of pitch or asphalt in the summer heat. This spreading flow
was naturally radial or outward from the center, and consequently
the direction of flow of the Erie ice mass over our district was from
the northwest. The margin of the ice was at right angles or normal
to the direction of flow, and hence extended northeast by southwest
along the northwest-facing land slope. As the recession of the ice
front was very slow it reposed for ages (we have no way of measuring
the time) against the steeper part of the valley slope, and its
position there, slowly falling or backing away, is indicated by the
lines of rock rubbish or moraine drift dumped at the ice margin, |
and by the stream channels cut by the drainage past the ice front.
Other belts of moraine farther landward mark earlier pauses in the
ice retreat [see fig. 1, p. 12].

(3) The drainage. If the reader now apprehends the relation
of the ice body to the general land surface (a huge ice mass filling
the bottom of the Erie valley and resting against the northwest-
facing land slope with its margin extending along the horizontal
contours of that slope) he will appreciate the fact that the stream
flow of that time must have been very unlike the present. On the
higher, exposed land surface the streams must have flowed down
the slopes (northwestward) as they do today. But the ice front
opposed their course and they could pass neither through, over,
nor beneath the glacier; they could flow only alongside or past
the ice margin. This land drainage along the ice border was
augmented by the abundant water derived from the melting of the
ice body itself.

The question will now arise as to the direction of escape for the
waters, whether to the eastward or westward. It has been found
that the eastward escape was impossible, not only because the
neighboring land is higher in that direction, but for the reason that
at this stage in the glacial retreat the Ontarian ice lobe was pressing
against the high ground in central New York. The escape was

GLACIAL WATERS IN THE LAKE ERIE BASIN It

southwestward along the ice margin to the open lake waters in the
- western part of the Erie basin, with ultimate overflow to the
Mississippi. This brings us to the matter which is the special
subject of this writing—the history of the glacial waters, the
stream phenomena and the lake records.

(4) The lake waters. As the ice body melted away, obliquely,
from the land slope the lake waters crept in along the ice margin
and occupied all the open space below their level. Beaches, as
gravel bars and spits, and delta fillings mark the borders of these
glacial lakes, which followed the waning ice front and expanded
to vast extent. Before we can fully and properly describe the
stream channels and the greater glacial lakes and their effects it is
necessary to discuss some other features, specially the moraines
and the local glacial lakes which occupied at various levels the
valleys sloping toward the glacier.

ICE MARGINS: MORAINES

The glacial period probably included several epochs of ice
invasion with intervening epochs of ice retreat or deglaciation. In
western New York we have accepted evidences of only the last epoch
of glaciation, called the Wisconsin. All the phenomena described
in this paper relate to or are connected with the waning and disap-
pearance of the Wisconsin ice sheet, and particularly of the Erian
and Ontarian lobes.

The pauses in the recession of the ice front are marked by termi-
nal accumulations of marginal drift, or recessional moraines. The
series of recessional moraines for the whole Erie.basin are given,
somewhat theoretically, in Leverett’s Monograph XLI. The corre-
lation of the later moraines in western New York with those across
the basin, in Ontario, Can. has not yet been made, although essen-
tial for full knowledge of the glacial lake history. The succession
and altitude of the glacial waters were determined by the successive
positions of the ice front, acting as a barrier, at certain critical
localities: As any possible mapping now of the correlated or cor-
responding moraines in Michigan, Ontario and New York would be
conjectural and probably misleading no attempt is here made to
map or represent them. ;

The terminal moraine, which marks the greatest expansion of the
Wisconsin ice body in the Lake Erie basin and western New York,
lies near Olean and Salamanca. From this locality it extends both
southeast and southwest into Pennsylvania, showing that the ice
front there had an indentation or reentrant angle.

I2 NEW YORK STATE MUSEUM

Between the terminal moraine and the present Lake Erie the
several recessional moraines are roughly parallel to the latter, or
have a general trend in the Erie basin northeast by southwest.
They decline or fall away to the westward and pass under the lake.
Of course they pass under the planes of glacial lakes Whittlesey and
Warren, whick are more than 200 feet above Erie. This fact is
shown in the sketch map, which also shows that the ice front was
convex westward, in the direction of flow.

Three factors combined to make the westward extensions of
these moraines weak and discontinuous. The glacial streams
flowing past the ice margins swept away more or less of the moraine
detritus within their reach, in some sections removing it entirely.
The portions of the moraines which were deposited under water were
spread out and subdued by the water action. Thirdly, the stretches
of moraine lying near the levels of the lakes were destroyed by wave
erosion and converted into beaches and water-laid drift. In
addition to these destructive effects during the glacial history are
those of weathering and rain and stream erosion during all subse-
quent time.

ay

'

Zl

Fig. r Diagram of the Erian ice lobe. The concentric lines indicate ap-
proximately the successive forms and positions of the margins of the ice,
as shown by moraines. The lines are generalized and are not intended
to be exact.

The Cleveland moraine, as named by Leverett, includes the irreg-
ular drift masses in the belt east and west of Chautauqua lake.
With this and the earlier moraines we have no special concern, as

Leta)

GLACIAL WATERS IN THE LAKE ERIE BASIN 13

they lie landward of the water-parting between Erie and Allegany
drainage and outside of our glacial lake territory.

The morainal belt which forms the divide or water-parting from
the Pennsylvania state line eastward, along the heads of Chautau-
qua lake and Cassadaga and Conewango creeks was called by
Leverett the Lake Escarpment moraine, a description of which
may be found on pages 654-72 of his monograph, with plates.
Streams of the glacial drainage [see p. 19] flowed along the landward
side of the Escarpment moraine in the stretch from the Pennsylvania
line to Chautauqua creek. Eastward the moraine is cut by trans-
verse outlet channels where the glacial waters held in the valleys
escaped across the divide (constituted by the moraine) to the
Allegany drainage. The drift-filled valleys heading in the moraine
at these outlets and leading southward, as shown on the map
[pl. 2], are remarkable features.

West of the meridian of Fredonia the Escarpment moraine is the
last one now existing, as below this the north-facing slope was all
swept by glacial streams or washed by the lakes, and the debris
which the ice had dropped was removed or scattered by the waters.
East of this meridian other and later morainic belts occur [see pl.
3-61.

The next succeeding moraine has been named by Leverett the
Gowanda. Appearing in fragments east of Fredonia it curves
around to Forestville and then swings eastward to the Cattaraugus
valley at Gowanda, whence it passes northeast to join the
broad interlobate moraine tract in Wyoming county. Near
Fredonia we find interesting evidence of the destroyed moraine.
Lying 2 miles east of Fredonia in the Belmore (Whittlesey) beach,
close to the west side of the Townline road, is a conspicuous mound
of till [see pl. 7]. It is evidently an erosion remnant of a frontal
moraine which has been mostly removed by Whittlesey waves and
Prewhittlesey drainage. Three fourths of a mile southwest from
this knoll is another less prominent till mass by four-corners.
Doubtless these fragments represent the southwestward extension
of the Forestville moraine.

Another belt of moraine which extends northeast from Hamburg
has been named by Leverett after that village. As suggested by
him, the ice margin probably extended southwest from Hamburg
but the drift was removed or leveled by the glacial waters. An
isolated tract of moraine of about 2 square miles area, lying midway
between North Collins and Irving and 2 miles north of Cattaraugus
creek, probably belongs to the Hamburg moraine. This lies be-
neath or lower than the Warren plane. which south of Brant and west

14 NEW YORK STATE MUSEUM

of Fenton has buried the moraine. Between Brant and Hamburg
the moraine is either washed away or buried. East from Hamburg
the moraine belt widens rapidly. It les north of East Aurora and
south of Alden and passes eastward into Wyoming county.

The Marilla moraine of Leverett is, at least at the west end, only
a part of the Hamburg moraine. The distinction which is based
on a line of glacial drainage is not valid, as the whole breadth of
the moraine has been cut equally by the streams past the ice front
[see pl. 5]. The Hamburg moraine extends north to the Warren
beach all the way from Hamburg east to Alden, the beach forming
the present northern edge of the moraine. The Whittlesey beach,
which is weak here, lies on the moraine.

Lying farther north and running east and west on the north-
facing slope of the Ontario basin are belts of moraine drift which
Leverett has named in successive order northward, the Alden
moraine; Pembroke ridges; Batavia, Barre and Albion moraines.
The two last are on ground lower than the surface of Lake Warren
and consequently do not figure in the history recorded in this
paper.

Two of the moraines named above correlate with events in the
lake history. While the Hamburg moraine was forming, Lake
Whittlesey was destroyed and was succeeded by Lake Warren, as
described in a later chapter [see p. 64]. No evidences of lake action
at the Whittlesey level are found beyond the Hamburg moraine, east
of a line joining East Aurora and Alden. With the removal of the
ice front from the Batavia moraine and from the limestone escarp-
ment east of Indian Falls the Warren waters were allowed to pass
eastward into central New York.

All of the moraines between and including the Escarpment and
Batavia moraines have been cut and channeled by stream work
past the ice front, while their western extensions have been sub-
dued or even buried by lake action, in consequence of which they
are imperfect on all the territory lakeward of the divide. Leverett’s
divisions of the moraine belts do not sufficiently recognize this fact.
If there had been no removal of the moraine drift it would be
impossible to distinguish all the belts named above. For example,
east of East Aurora the Gowanda, Hamburg and Marilla moraines
are virtually only a single‘moraine, cut by stream channels through-
out its entire breadth. The Gowanda belt is probably only the
northern edge of the Escarpment moraine; and the Marilla is the
same part of the Hamburg moraine.

Mention has been made of isolated fragments of the eroded
moraines. Others will be seen on the maps; particularly a mass

‘req Aasopqity \\ 2Y} WoO Spueyzs esnoy ey, ~“AasayqqIYy AA OMe] pUv oSevurerp [erowls Aq poyeroz}qo AT}sour useq sey Yor
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GLACIAL WATERS IN THE LAKE ERIE BASIN 15

2 miles southwest of Portland,-and one 2 miles northeast of
Brocton. All these fragments should correlate with recognized
moraines.

The close association of the moraine deposits on the land slopes
facing Lake Erie with the scourways of the glacial drainage and the
work of the glacial lakes must be clearly recognized in order to

understand the various and intricate phenomena. The several

maps suggest this intimate relationship.
GLACIAL DRAINAGE CHANNELS

These effects of the glacial waters are not so prominent as the
lake shores but are much more widely distributed. They are
not so conspicuous features to the untrained eye as the bars and
continuous beaches, but when once recognized they are unmistaka-
ble. The more definite channels are valleys or notches or terraces
of various sizes, in either rock or drift, and with or without present
streams. The stronger of them are evident-in their origin, having
all the characters which distinguish the work of streams, namely,
fairly uniform grade and width, curves with radius proportionate
to size or strength of stream, definite banks, and with correlating
areas of drainage on the one hand and receiving water bodies on
the other. All gradations will, of course, be found down to small,
shallow and indefinite scourways made by short-lived currents,
even to those of doubtful origin. Along steep slopes the stream
cutting is commonly shown only by more or less decided notches
or shelves or terraces in the slope, the ice having been the lower
wall of the channel. The removal of the ice has in these cases left
us the anomaly of water courses with only one confining bank,
the down-slope wall being, so to speak, in the air. We need to
restore the bank of ice in our imagination. Plates 2-6 give the loca-
tion of these ancient and extinct channels. It must not be thought
that the water channels are unique or peculiar to this region,
for they are found wherever the great glacier was holding bodies
of water in depressions of land slopes. They occur not only through-
out the entire district described in this paper but eastward along
the south slope of the Ontario basin to Rome and down the Mohawk
valley to Little Falls. The largest glacial channels in New York
lie in the Syracuse region, with huge cataracts that rivaled Niagara
in size and were the predecessors of Niagara in fact, as they carried
the falling Warren waters eastward to lower levels.’

1 Descriptions of the channels and cataracts in the Syracuse district and
eastward will be found in papers by the author in the 2zoth, 21st and 22d
annual reports of the New York State Geologist.

16 NEW YORK STATE MUSEUM —

Across the main divide to Allegany drainage

The reader should clearly appreciate the relation of the ice body
to the general land surface. While the ice margin was lying on
ground having free southward drainage the waters utilized the
valleys leading south and away from the ice front and they had no
occasion for making new channels. The copious waters from the
summer melting of the ice mass, combined with that from the

local rain and snow fall, produced heavy floods in the south-leading

valleys; and vast quantities of debris from the ice were swept
far down the valleys and filled them to great depths. This is
well illustrated in the valleys of Cassadaga and Conewango creeks
as shown in plates 2-3. The present creeks meander listlessly
over the broad plains of valley-train drift left by their larger
glacial predecessors, and are contributing only a surface layer
of fine materials or are intrenching themselves in the older deposits.

When the ice front receded to the northward of the divide the
waters which were then ponded in the valleys facing the ice had
to escape across the divide, through the lowest passes or cols,
which were often deepened or cut down by the water flow. The
divide was usually formed, at least in the valleys, by the moraines
left by the ice, and in our district the transverse channels are in drift
and not in rock.

The general ice front adapted itself to the larger land configura-

tion, and lobations of the ice pushed forward into the greater —

valleys, as shown in figure 1 for the Erian lobe. It will be seen
that the broad relation of the ice and land was such that the south-
leading channels were, in general, opened successively from west
to east; but the precise relation in time is uncertain and is not
important here. These channels will be enumerated here very
briefly and discussed again in a later chapter in connection with
the local lakes which they drained.

The south-leading outlets for the glacial waters held in the basin
of the Genesee were described in 1896. The Genesee lakes lay
on the eastern border of the territory described in the present
paper, and the more southerly of the Genesee outlets were probably
effective while the ice was yet lying over all of our area. Probably
some of the small primitive lakes held by the ice in the eastern part

of the Cattaraugus basin were tributary for a time to the Genesee

waters, but these details have not been studied.

The easternmost channel which carried only Erie basin waters
is probably the one at Machias, in Cattaraugus county, with eleva-
tion of 1646 feet. This was the outlet of the glacial lake in the upper

1Glacial Genesee Lakes. Geol. Soc. Am. Bul. 7:423-52.

GLACIAL WATERS IN THE LAKE ERIE BASIN 17

part of the Cattaraugus valley. Some 6 or 7 miles west of the
Machias outlet is a pass near West Valley with altitude over 1700
feet which could have been the point of overflow of only the local
waters of the Ashford creeks since it was higher than the Machias
outlet that was already open.

The next effective channel, later in time and lower in altitude,
is at the Persia flag station between Dayton and Cattaraugus
stations of the Dunkirk branch of the Erie Railroad, some 7 or 8
miles southwest of Gowanda. The head or intake of this channel
is close to the steep west bank of the south branch of the Cattaraugus
‘creek. The water-parting is a swamp and the channel is about
1 mile wide. The channel leads northwest 4 mile, where the rail-
road crosses it by a low filling, then curves around sharply to
the southwest and opens into a valley tributary to the east branch
of the Conewango. As it is about 300 feet lower than the Machias
outlet it probably succeeded the latter as the outlet of Cattarau-
gus glacial waters.

All the other outlet channels which carried waters from the Erian
basin over into southern or Allegany flow are represented in the
accompanying maps, except possible points of overflow west of Chau-
tauqua lake in a district not yet surveyed for the topographic map,
but which are doubtless inconsequential as the waters could have
formed only small lakes close to the divide.

In the district between Mayville, at the head of Chautauqua
lake, and Westfield, near Lake Erie, there is an interesting com-
plexity of the drainage, shown in plate 2. The branches of Chau-
tauqua creek (which has no relation to the lake of that name but
drains the Erie slope, passing northwest through Westfield) have
cut three deep “‘gulfs’’ in the Portage shales and the features
which were left by the glacial drainage are somewhat obliterated.
The earliest and highest overflow of the glacial waters in this
district is shown on the map as 3 miles west of Mayville, with
altitude according to the map contours under 1380 feet, the waters
escaping east to Chautauqua lake. A later, lowerand more important
southward outlet for the waters of the ancient Chautauqua creek
valleys is a broad swamp col at the head of the Little Inlet creek,
24 miles north of Mayville, with map altitude 1320 feet. These
cols must have been uncovered by the ice retreat so nearly at
the same time, judging by their relation to the general slope, that
the earlier and higher outlet could have been effective only a
relatively short time.

18 NEW YORK STATE MUSEUM

Four miles north of Mayville and over a mile southeast of Pros-
pect station on the Pennsylvania Railroad is a short channel by the
four-corners at the ‘‘“Elm Flat” church, with altitude of 1340 feet.
This is at the head of the swamp in the “big inlet”’ of Chautauqua
lake and could have carried the overflow of only a limited area and
_ for a short time.

The next outlet is at the head of Bear lake valley, 3 miles south-
east of Brocton. This is a broad swamp col, still in timber, with

map altitude of 1320 feet, which carried a heavy drainage for

some time. The close correspondence in present altitude between
these several channels is probably merely coincident. The north-
ward tilting of the region in Postglacial time has lifted the
Bear Lake outlet 10 to 15 feet higher, as compared with the Big
Inlet pass, than it was when effective.

The col 5 miles south of Fredonia, between the heads of Canada-
way and Cassadaga creeks, must have been the overflow point for a
large volume of water. It lies close to the Upper Cassadaga lake
in the valley moraine with altitude not much over 1300 feet, but
does not exhibit clear channel characters. This seeming incon-
sistency and the peculiar features and relationship were discussed
in the zoth Annual Report of the State Geologist, pages 132-35.

Passing eastward we find three groups of cols at the heads of
three branches of the Conewango creek [see pl. 3]. The only well
defined channel is on the western col, 14 miles west of Mud lake in
the town of Arkwright. The waters of Walnut creek valley found
escape here over to the west branch of the Conewango at altitude
of 1420. While the drift filling of the broad south-leading valleys
shows that they carried heavy detritus-laden floods from the melting
ice front, it would seem that little water passed across the cols into
the valleys of the North branch and the Slab City branch of the

Conewango, apparently for the reason that the conformation of the
ice front to the topography was such that little was ponded here
north of the divide. From south of Forestville eastward to Perrys-
burg no basins faced the ice front and the drainage was fairly free
past the ice to the westward.

No other cols across the main divide between Erie and Allegany
waters have any relation to the glacial overflow in our district. The
passes at the heads of the several strong north-sloping valleys in
Erie and Wyoming counties simply carried their waters over to the
Cattaraugus basin, from whence it found further escape by chan-
nels above described. Three miles northwest of Cherry Creek is a
fine channel which was the outlet to Farrington Hollow glacial
lake, but both features are wholly in southern drainage.

0 tted a eid

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ey SUE Ital

GLACIAL WATERS IN THE LAKE ERIE BASIN ie)

Along the ice front westward to Erian waters

West of the Cattaraugus embayment. State Line to Westfield
[pl. 2]. In this section the Escarpment moraine lies against

the steep valley slope, to the extent that it has not been swept

away by the glacial waters. The most definite and strongest
stream channel of this class lies south, or landward, of the Escarp-
ment moraine, south of Ripley, and at altitude of 1400 down to
1200 feet and lower. About 3 miles of the upper part of this ancient
channel is shown on the Westfield sheet, and its continuation appears
on the Clymer sheet. It has been deepened by modern drainage
and is now occupied by the north branch of Twentymile creek. As
a deep ravine the channel continues southwestward into Penn-
sylvania and swinging west and northwest crosses the railroads a
mile west of State Line [see fig. 2].

The considerable stream which cut this large channel carried not
only the waters from a long stretch of the melting ice front for a
long time but also the land drainage of a large territory, and the
latter service is continued by the present stream.

When the ice front finally melted back from the summit and
rested at lower and lower levels against the steep land slope the
drainage lay usually close against the ice front, following the latter
in its retreat, and made few noticeable channels west of the West-
field meridian. The only one mapped near Ripley is about 14
miles southeast of the village, crossing the highway that climbs the
slope, at 1200 feet by the map.

Along this steep slope above Ripley and for several miles to the
northeast the moraine drift was mostly removed by the stream
work past ,the ice, the characteristic morainal features being found
in patches and more at the foot of the steepest slope. The modern
drainage has also helped to destroy the old drainage lines and the
drift deposits.

On the west side of the “Gulf,” 3 miles south of Westfield, are
three gullies leading eastward which have been partly cut, along
with the “Gulf,” by recent drainage. However, they were probably
initiated by the glacial waters flowing intothe primitive valley of the
“Gulf”? and then on across the divide into Chautauqua lake by
channels already described. These east-leading channels have their
heads at about 1400 feet, and lie on the landward side of the moraine.
They are unique in being the only cases found in the Erie district
where any drainage along the ice front was not westward; and they
really belong to the early overflow across the divide to southern
drainage.

20 NEW YORK STATE MUSEUM

South of Westfield, 2 and 3 miles, west of Chautauqua creek and
also between the gulfs, the old glacial stream work is conspicuous.
This isshown very well on the two north and south roads west of the
creek, at altitudes from tooo down to 820 feet. On the two ridges
between the three ravines the crosscutting by the glacial flow is
very striking. The general surface is morainal but the knolls are
cut into terraces or even into double-walled channels. On the east

ridge cuts are found at 880, 960, 1020, and an excellent channel at

1200 feet (by the map contours), above which is a strong remnant
of the moraine. Correlating with these cuts on the east ridge are
others on the west ridge, naturally at a lower altitude, while those
already noted as lying on the north and south roads west of the creek
are in continuation of the same flow. This series of interrupted
channels converges toward Forsyth, where the stream flow de-
bouched into Lake Whittlesey and produced the delta deposits
which have chiefly been built into the broad beaches of Whittlesey
and Warren.
Westfield to Portland. One and one half miles southeast of
Westfield is a series of east and west scourways which lie at alti-
tudes of about 850 up to 1000 feet, according to the somewhat un-

reliable contours of the map. These channels probably represent |

in part the same flow as the lower cuttings southwest of the village.
Evidence of stream work is also found along the higher slope farther
southeast, up to 1200 feet. Several strong and sharp stream-cut
notches and channels occur on the north and south roads north,
west and south of Prospect station, 24 to 34 miles east and northeast
of Westfield. There are at least seven of these channels, ranging
from 860 up to 1300, and allin rock. The detritus borne by these
streams probably supplied part of the material of the broad sand
plains east and west of Westfield. Further representation of these
channels is found northeastward along the tracks of the Pennsyl-
vania Railroad as shown on plates 1 and 2.’

Portland to Fredonia [pl. 2]. Extending from Portland southwest
for 3 miles to West Portland church is an extended delta, lying be-
tween the Whittlesey (Belmore) and the Warren (Forest) beaches,
and also landward. The explanation of this broad gravel deposit is
found in a river channel which debouches south of Portland and

‘Explanation. The interrupted character of the stream channels as
represented on the maps is not wholly true to nature but is partly due to the
fact that they have been mapped only where actually observed, chiefly along
the highways, and are not indicated hypothetically. It would be a tedious
labor to trace all the scourways throughout the Erie district. Students
interested in the subject can appropriately trace and map the features in
precise detail in special districts. The author will be very grateful for such
information.

>

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GLACIAL WATERS IN THE LAKE ERIE BASIN Pat

"which has been traced upstream for 8 miles to the Canadaway valley
_ south of Fredonia. The head of this river channel lies within 4 mile
of the Shumla reservoir and nearly 3 miles south of Fredonia. It
_ here forms a dry gorge, about 100 feet deep and 2 miles long, known
locally as Wheeler’s gulf [pl. 8-10], and utilized for grade by a
' detour of the Dunkirk, Allegany Valley & Pittsburg Railroad.
_ Beyond this gorge is an open section of about 4 mile in length below
_ which the channel forms another gorge 14 miles long, ending a mile
; south of Lamberton. For the remaining 4 miles to Portland the
channel lies just above and landward of the Whittlesey beach.
' The head of the river channel is t100 feet in altitude and the de-
bouchure is 800 feet. ;

Some traces of stream cutting earlier and higher than the
Wheeler’s gulf channel have been noted southeast of Portland, and
such must occur along all the slope to the northeast, which is quite
destitute of morainal drift up to about rooo feet.

Above Wheeler’s gulf higher scourways are seen, one of which is
tributary to the gorge. Below the gulf, on the Fredonia meridian,
all the slope from rroo feet down is swept bare to the rock, and a
series of rock shelves head at Io050, 1000, 960, goo and 860 feet by
the map, declining westward. The higher ones converge and unite
with the Wheeler’s gulf channel south of Lamberton, but the lower
ones debouched into Lake Whittlesey east of Lamberton and
helped to form the delta deposits south of the village.

Fredonia to Forestville [pl. 2-3]. The stream cuttings which head
south of Fredonia carried waters which were ponded in the Canada-
way valley at levels corresponding to these outlets. We may call
these waters the Shumla lakes, after the hamlet in the valley. The
depth of the lake when Wheeler’s gulf was the outlet was about 200
feet, and the breadth about 1 mile. The reader will appreciate the
fact that the lakes must have been fed by glacial drainage past the
ice front from the east, and the proofs of such action are abundant.
From below Shumla to below Laona, about 2 miles, the east. wall of
the valley holds a great volume of delta deposits banked against the
slope. The higher of these form conspicuous terraces, visible for
miles and plainly seen from the railroad. These have an elevation
under rroo feet, thus correlating with the lake level when this was
fixed by the Wheeler’s gulf outlet. But the delta deposits extend
down the valley to Fredonia through all levels to 750 feet, the lowest
level of Lake Warren.

The conspicuous delta terraces in the valley east of Laona were
built in the Shumla lake by the rivers from the northeast, the

22 ,NEW YORK STATE MUSEUM

strongest channel, about 24 miles long, heading in the south edge of
Sheridan township, at 1260 feet altitude, and debouching at the
delta as low as 1000 feet. The uniform slope facing northwest and’
lying 4 miles east of Fredonia is entirely denuded of drift and
strongly terraced by stream work, similar to the slope south of Fre-
donia. The highest stream work noted lies above the Laona chan-
nel, at altitude over 1300 feet, and the lowest is the broad, smooth
scourway facing the Whittlesey beach at altitude about 840 feet.
Theoretically there must have been westward flow of water on this
slope at 1400 feet, or just inferior to the outlet across the divide to
the Conewango, at the head of the Walnut creek valley with ele-
vation of 1420 feet; and such flow 1s indicated on plate 3.

West and southwest of Forestville the land slope has more
irregular surface and the stream cuttings are intricate. From the
Walnut valley, where the waters were ponded in a lake which we
will call the Walnut lake, the waters escaped westward between low
hills forming a series of scourways with oblique directions, as shown
in plate 3. The lowest is at the foot of the hill west of Forestville
and not much above the Whittlesey level. South of Sheridan
station a portion of the Gowanda, or Forestville moraine lies land-
ward of the beach for a stretch of 3 miles, and the lowest stream
work cuts the moraine. On the north and south road south of the
station two narrow channels intersect the moraine. The detritus
carried by the streams along this section helped to make the delta
deposits south of Fredonia and the massive beaches northeast of
the town. ;

Forestville to Gowanda [pl. 3]. This section of the land slope
swings around into the Cattaraugus valley with change of face from
northwest to northeast. The earlier waters were the overflow of the
Cattaraugus lake into the Walnut lake. The stream cutting is
complex and the reader should consult the maps. Northeast of
Forestville and east and west of Smiths Mills the channels are
strong and deep cuts in the rock.

The highest flow on the northeast slope can not be over 1300 feet,
since the Persia outlet [see p. 17] of the Cattaraugus lake was not
much over that hight. The highest stream work noted is close to
Perrysburg, at elevation by the contours of 1300 feet. Local waters
in the Walnut basin cut channels southeast of Forestville as high as
1400 feet. As in other regions already described the slopes show
little morainal drift, this having been carried away by the glacial
streams.

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GLACIAL WATERS IN THE LAKE ERIE BASIN 23

From Forestville northeast to Smiths Mills station, nearly 4 miles,

"the rock terraces cut by the glacial flow along the ice front are very
conspicuous and can be clearly seen from the Erie Railroad which
crosses them obliquely.

In the region of Smiths Mills the irregular ground has been cut

into pronounced channels or gorges, and the detritus has been

swept into the delta fillings in the Walnut valley at Forestville and
northward.

It will be understood that the broken appearance of the channels
on the maps, specially the higher ones, is partly due to want of com-
plete knowledge, as they are rarely denoted on the maps unless
actually seen, which is mostly on the highways. Interpolation of
hypothetic cutting is indicated by broken bands. However, the
channels are not usually continuous for long distances on irregular
slopes, or where the ice front was oblique to the slope.

East of the Cattaraugus embayment. Gowanda to Hamburg’
[pl. 4]. Over the territory thus far considered we have the help of the
topographic sheets. The remaining territory, about one half of
the whole area, has been studied at great disadvantage with the
aid only of county and road maps. The altitudes given are mostly
by aneroid and are only closely approximate. The channels are
indicated only where seen, mostly along the ae and the
following descriptions are very general.

In the southern half of this section the land ape) faces west,
and the glacial stream flow was southward. Toward Hamburg the
slope faces northwest, while south of the village it faces north.

The highest scourways in this section were determined by the
hight of the cols at the heads of Eighteenmile creek, leading
over into the Cattaraugus at Wyandale and eastward. These cols
have not been positively determined and no attempt has been
made to locate the very highest scourways. The important and
interesting fact is proven, that all the steep slopes north of Shirley
have been water-swept and cut into notches or terraces, and the
morainal drift removed. The stream cuttings are more commonly
shown as terraces than as double-walled channels, but this dis-
tinction is not always indicated on the map.

From Gowanda north to Shirley, a distance of about 8 miles, the
slopes bear scattered morainal or kame knolls, which proves that
this slope has not been severely stream-swept. The reason for this

1In the study of this section the writer has had the assistance of Mr B. W.
Law, whose summer home is near Collins. His observations are incorporated
in this writing without special designation, but with this grateful acknowledg-
ment.

24 NEW YORK STATE MUSEUM

exemption seems to be as follows. Until the lobate ice front had —
receded from the Cattaraugus valley as far as Shirley in this dis-
trict the waters in the Cattaraugus embayment were held as high-
level lakes, having their outlets across the slopes north and north-
west of Perrysburg. In this case no stream flow could occur
along the ice front in the Shirley district or on the slopes north of —
Gowanda until the lake waters were drained to a level lower than
the ice border. The kames (knolls of sand and gravel) which are
scattered over the slope from Collins north to Shirley were pro-
duced by glacial streams debouching into standing water that
faced the ice border. The reader will appreciate how such phen-
omena as these, along with the relationship in series of the
stream channels and deltas, enable us to determine the position
of the receding ice front and to find the relationship or correlation
of the several features.

On the road leading east from Shirley there are some weak scour-
ways which suggest glacial drainage, but are not strong enough
to map with confidence. Northeast of Shirley and east of North
Collins some scourways, not very strong, are indicated on the map
[pl. 4].

The lowest stream work at North Collins is a steep bank facing
the Whittlesey beach east and south of the village, at altitude about
850 feet. The highest channel noted is 2 miles east of the village,
near four-corners, with altitude over 1100 feet.

At the three-corners.14 miles south of Eden are interesting
channels cut in black shale, with remnants of the rock left as
islands or outliers. One mass is exactly at the corners; another
lies south with a ridge form; and small ones occur on the west
side of the road. .

The Whittlesey shore in this section lies frequently along cliffs
of rock which may have been partly cut by glacial stream work
before the wave work by the lake. Examples of these cliffs may
_ be seen in North Collins; and east of the ridge road for 3 miles
south of Eden, and for a mile north of Eden.

Strong channels in rock le north, south and west of East
Eden. About a mile north of the village and just south of the
Lutheran church are two fine channels. West and northwest of
North Boston the slopes are cut; and the conspicuous Whittlesey
cliff 2 miles southeast of Hamburg was probably made partly by
stream action.

The detritus carried by the streams at North Collins was probably
swept into the Cattaraugus valley below Gowanda. The channels

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GLACIAL WATERS IN THE LAKE ERIE BASIN 25

south of Eden may have contributed detritus to the sand plains
r, west of North Collins; while the deltas at Eden and Eden Valley
“were built by the later drainage south of Hamburg.

Hamburg to East Aurora [pl.. 5]. In this section, lying
_ between Eighteenmile and Cazenovia creeks, the stream phenomena
become more complex, as the land slope is not steep and the surface
' is dissected by large creeks. The maps show the observed channels.
_ The highest channel noted is 4 miles due east of Hamburg, and
4 Over I1o0o feet altitude. The lowest channels are apparently
- connected with Whittlesey lake erosion.
_ At the four-corners, 24 miles east of Armor and 2 miles south of
i Orchard Park, is a heavy bluff, pictured in plate 12, which is a con-
_ tinuation of the large channel 2 miles southeast of Orchard Park,
_ crossing both the highway and railroad with a southwest direction.
_ The head of this river course is a channel 3 miles west of East
Aurora at Longs Corners, on the ‘“‘Quaker”’ road, figured in plate 13.
It lies just south of the three-corners, with direction nearly east
and west; the bluff being 35 to 4o feet high, in rock, and the clear
channel 10 to 15 rods wide. The head of this cut lies across the
east and west road with a scourway 20 rods wide. The total
length of this river channel is something over 5 miles.

south of East Aurora the slopes are smoothed and broadly
terraced by water flow, carrying the overflow of the east branch
valley of Cazenovia creek, but the scourways are not definitely
mapped.

The detritus carried by this eastward drainage from the Caze-
novia creek was contributed to the broad delta filling on which
Hamburg stands.

East Aurora to Cowlesville [pl. 5]. This section, extending
from Cazenovia creek to Cayuga creek, has a most interesting

_ development of moraine, channels and deltas, and the phenomena
are complicated by the change of base level from the Whittlesey
to the Warren plane. In all the territory thus far described,
lying westward to Pennsylvania, the stream phenomena ended at

_ the Whittlesey level, as that lake water was the receiving body
and the base level of drainage. While the ice front was lying in
this section the outlet of Lake Whittlesey across the ‘‘Thumb”’
of Michigan was abandoned [see p. 42] and the lake waters were
lowered to a new outlet, thus establishing Lake Warren. East of
Marilla the lower stream channels are cut down to the Warren plane.
Delta fillings at the Whittlesey level occur in this section, but are
not found further eastward.

26 NEW YORK STATE MUSEUM

In this section a series of vigorous creeks flow to the northwest
in parallel courses: Cazenovia creek at East Aurora, Buffalo creek
at Wales and Elma, Little Buffalo creek at Marilla and Cayuga
_creek at Cowlesville. Standing waters were held by the ice barrier
in each of these valleys and the inflowing streams dropped their
detritus at varying levels, the larger delta plains ranging from
somewhat above the Whittlesey level, or at about 920 feet, down
below the Warren level, or to about 820 feet. (The Whittlesey
shore at Elma Center station is 905 and the lower Warren 835 feet.)

There is an important difference between this section and those
west of Hamburg. Here we do not find a steep rock slope from
which the morainal drift has been swept, but we find instead a
broad frontal moraine of usually sharp relief and dissected by num-
erous streams of the glacial drainage. On the meridian of Williston
the moraine has a breadth of about 8 miles, from Wales Center to
West Alden, and all the central part for a width of 5 miles is cut
by conspicuous channels which carried the ponded waters westward
from one valley to the next. The altitude of these stream channels
declines, of course, along any meridian from south to north suc-
. cessively, although the. difference between two successive cuts
may not exceed io or 20 feet. The number and closeness of the
channels are well seen on the four north and south roads from
Marilla eastward. -

Our interpretation of the moraines in this section is somewhat
different from that given by Leverett [Monograph XLI, pl. XXV,
p. 673-84]. He separates the moraines by broad belts of drainage
into the Gowanda, Hamburg and Marilla moraines. The writer
does not find such important concentration of the old drainage,
but that on the contrary the channels are so numerous and widely
distributed that the moraine can not justly be divided. For its
entire width from East Aurora and Wales Center north to the War-
ren shore the moraine is essentially a unit.

Southeast of East Aurora nearly 3 miles are two scourways
lying against morainal knolls at altitude of about 1140 to 1180
feet. Other westward outlets of the waters held in the Buffalo
creek valley over Wales should occur at lower levels.

East Aurora lies on a broad delta filling built near the Whittlesey
level. The head of the plain east of the village is about 925 feet.
The Pennsylvania Railroad station is given as 921 feet. Down-
stream, or westward, the plain declines to under goo feet. On the
north of the village, between the delta plain and the south edge
of the Hamburg moraine, is a channel some 60 rods wide with the |

Plate 12

Looking eastward (upstream)
BE

plate 1

Continuation of channel shown in

Bed and south bank of glacial river, 24 miles south of Orchard Park, near four corners.
from the north-and-south road.

-

GLACIAL WATERS IN THE LAKE ERIE BASIN 27

steep north bluff in till, 4o feet high. This channel would seem to
be the latest and lowest, on this meridian, of the glacial drainage.
_ It was the western extension of two glacial channels from the east.
The higher of these forms a cut bluff at the three-corners on the
Townline road, 2 miles northeast of East Aurora. Its westward
continuation is seen leading southwest, south of the Marilla Street
_ road, nearly to the village where it meets the present drainage.

Another lower and broad channel crosses the Townline road a little

distance north of the former, and south of the next three-corners,

and leads west into the indefinite swampy tract a mile northeast
of the village and which forms the head of the capacious channel
north of the village.

Between the two old channels above noted lies a delta gravel
plain which supports the Marilla Street road. This plain is much
pitted along its northern margin, showing that it was deposited
against the ice front; masses of the ice being buried in the gravel,
their subsequent melting produced the basins or “‘kettles’’ in the
plain.

East and northeast of East Elma, and curving around from
north of Porterville to near Marilla, is another extensive and
interesting delta plain. The northern margin certainly lay against
the ice front, as is proven by the kettles or “pitted-plain” surface.
At least nine glacial streams from the east share the responsibility
for this deposit, the channels being distributed for 3 miles along
the north and south road between Porterville and Marilla. The
debouchure of the higher channels and their relation to the delta
show clearly from the highway. The varying altitude of this
multiple delta plain, 920 to 940, seems to correlate with the Whit-
tlesey waters, which in this region had their greatest eastward
extension with an altitude over 900 feet. This broad delta lies
above and east of the hamlet of East Elma, and we will call it the
East Elma delta.

The latest ice border drainage on this meridian has left two
channels east and northeast of Marilla. The earlier of the two
streams cut a conspicuous bluff back of the cemetery, southeast
of the village, and also a channel about a mile southwest of the vil-
lage, leading over to Buffalo creek at the Warren level. Marilla
lies on a delta. The upper terrace, about 860 feet, may have been
partially formed at the ice front in local waters connected with
the glacial streams just noted, but as a plain of the ancient Little
Buffalo creek the gravel terrace continues 14 miles northwest
into the Warren delta plain, capped with wave-built bars. The

28 NEW YORK STATE MUSEUM

later of the glacial streams here seems to have dropped its detritus
into the Warren flood.

In this region, therefore, we find the critical relation of the ice
front to the changing lake levels; the lowering of the base level of
drainage from the Whittlesey to the Warren waters, or from ~
about gto to about 860 feet. The Marilla delta is the most westerly —
delta built by glacial drainage close to the lake shore with a level ©
below the Whittlesey plane.

The change in the level of the dtemane is more abrupt than ~
would be expected. It is not supposed that the broad Lake ©
Whittlesey could fall suddenly to the Warren plane, but the ice ©
front seems to have held so steadily here that the relation of lake ©
level to inflowing streams changes abruptly, or within a short 7
distance. Two miles southwest of Marilla the extended East ~
Elma delta is over goo feet altitude. At Marilla the delta is at —
the Warren level, 860 feet. The channels of ice border drainage
1 mile south of Marilla terminate at goo to 940 feet. The channels
at and southwest of Marilla are down to 860 feet. There seems ~
no doubt that the higher channels debouched into Whittlesey
waters; the lower into Warren waters.

An unusual display of ice border drainage is seen on the four
north and south highways between the meridians of Marilla and
Alden. On the road through Williston not less than nine channels
are mapped, spaced through about 5 miles. The earliest and
highest channel that has been noted on the Williston meridian is
3 miles south of Williston, leading over to Buffalo creek at Wales
Center, with an altitude of 1100 feet. The lowest channel is at
four-corners, 2 miles north of the village, where three primary
channels lie athwart the north and south road and unite into one
Tiver course (the later of the two at Marilla) which carried the
waters from the Cayuga creek valley (the Cowlesville lake) over
to the Warren level at Marilla. The earliest flow through the
upper course of this channel may have helped to cut the cemetery
bluff at Marilla; and the later flow contributed to the lower delta
terrace at Marilla in an embayment of Lake Warren.

The earliest and highest channels in the territory included in this
chapter (between Buffalo and Cayuga creeks) lie east of the meridian
of Cowlesville, since the Cayuga creek flows northwest. The
highest channels actually seen and definitely mapped lie 1 mile
north of North Sheldon corners at 1400 feet altitude. A still
higher overflow should have occurred, somewhat under 1500 feet,
and scourways will probably be found + mile north of the corners.

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GLACIAL WATERS IN THE LAKE ERIE BASIN 29

_ At Bennington corners and westward, and west of Folsomdale,
the channels are excellently developed, specially the lower ones,
leading toward Williston, which are cut in the rock.

Cowlesville to Attica and Batavia [pl. 5]. This section of
country with its remarkable display of ice border channels lies
between the Cayuga and Tonawanda valleys, a diagonal distance
from Cowlesville to Batavia of 18 miles.

The highest known outlet is about 2 miles west of North Java, and
carried the waters of the Varysburg-Johnsonburg lake over to the
Java-Wales lake. This outlet channel heads where the railroad
makes the upper crossing of the Tonawanda creek, 14 miles west
of North Java, and leads west and southwest through a moraine,
14 miles, over to a branch of Buffalo creek which flows south from
Frink’s Corners. The aneroid altitude is about 1500 feet. (Some
higher stream work was seen in the village of North Java just
south of the corners. This evidently carried the overflow of the
North Weathersfield valley, a branch of the Tonawanda, westward
past the ice front and built a delta close to the village on the south-
west at over 1600 feet. This indicates that some temporary outlet

for the North Java waters existed on the west at an elevation
correlating with the delta, and superior to, and earlier in time than,
the channel by the railroad.)

The next lower escape to the west was by the channels north
of North Sheldon, already noted above. At this time a single
body of water existed in both the Tonawanda and Cayuga valleys,
since the broad swamp col at the head of Cayuga creek, near
Perry’s Crossing on the Buffalo, Attica & Arcade Railroad opens
into the Tonawanda valley at about 1380 feet.

When the overflow was lowered to the channels at Bennington
Corners, at and under 1360 feet, the Cayuga valley held a distinct
lake, the Humphrey Hollow lake, and the Varysburg-Johnsonburg
lake may have been tributary to it for a time oe overflow through
the Perry’s Crossing col.

The Varysburg-Johnsonburg lake found oe escape past the
ice border when ground was opened south of Bennington Center
with altitude below 1380. These channels are sharp cuts across
the north-south road, and terminate in conspicuous deltas south-
west of Bennington, with altitude 1300 down to 1200 feet.

When the ice front had retired sufficiently a new channel was
opened for the Tonawanda waters, the Kanawaugus valley, leading
across south of Poland Hill through Bennington to the Cayuga
valley east of Folsomdale. This is now a circuitous route and for

30 NEW YORK STATE MUSEUM

a time the ice front held the river flow to a more direct westward —
course by cutting across the brow of the hill south of Bennington.
Eventually the waters were ponded in the broader section of the —
Cayuga valley and an extensive delta was built above and below ~
Cowlesville. : :

The subsequent and lower escape of the Tonawanda waters
(Attica lake) over to the valley of Cayuga creek, and later
directly into Lake Warren, has left striking records of river flow
over a large area. This area is partly in the northern edge of
Wyoming county but chiefly in the southern part of Genesee
county [see pl. 6]. The Erie railroad follows one of the channels
in the midst of the series, and the Delaware, Lackawanna & Western
Railroad lies in a lower one at Ray station. The latest flow was
along the lines of the Lehigh Valley and the New York Central
Railroads. The entire area is covered by the Alden-Batavia
moraine.

All the north and south roads between Alden and Darien show
numerous waterways. The Countyline road, 1} miles east of
Alden, shows several channels. These unite into two channels
and debouch at Warren level near the village where they helped
to form the extensive gravel plain, crowned with strong Warren
bars. On the road passing through Darien Center 14 channels
are found worthy of representation on the map; and an equal
number lie on the next road to the east. The higher of these
channels are 1200 feet.

The lower ice border drainage in this region poured into Lake
Warren near Fargo station. The lowest lies along the south side
of the Lackawanna Railroad east of Fargo station, with altitude
about goo feet. This channel terminates as a cut bank or bluff 4
mile south of the station, facing the delta, the broad smooth g avel
plain that is bounded on the north by the railroad and on the west
by the Countyline road. Two strong gravel bars built by Warren
waves on the west margin of this delta lie across the north and
south Countyline road, 13 miles southwest of Fargo station, the
north one supporting the cemetery. These channels lying along
the Lackawanna Railroad have their heads north of Alexander and
pass through or south of Ray station. One and one half miles
west of Ray station and on the north side of the river channel is
a broad gravel plain that was deposited as an outwash from the
glacier, while the course of the glacial river which fed it is marked
in the strong esker or sinuous gravel ridge which partly supports
the crooked north and south road. The level of this plain, about

GLACIAL WATERS IN THE LAKE ERIE BASIN 31

940 feet, was determined by the hight of the water in the Ray
channel.

The latest glacial overflow from the Tonawanda valley was
across from Batavia through the indefinite channels in the Batavia
_ moraine now drained west by Murder creek. This overflow pro-

duced the broad delta plain northeast of Crittenden, which bears

a series of Warren bars [see pl. 5]. All the region 1s half buried

moraine. The contour lines of the Attica sheet show a vast number

of morainic knolls with their bases buried in stream and lake de-
posits. The network of swamps and indefinite water courses
attest the work of sluggish waters falling over into Lake Warren,
the primitive shore line of which is buried in this region. The

better defined stream channels are indicated on the map, plate 5.

They lie south of Batavia and West Batavia and south of the
_ New York Central Railroad to within 2 miles of Corfu, where they

swing north of the railroad and village and as noted above terminate

at the Crittenden delta, the south bank forming a bluff north of
the highway.

The lowest overflow at Batavia has an altitude of about goo
feet. The gravelly plain in the southern part of the town is 10 to
20 feet lower, and may represent some combination of leveled
kames, glacial outwash, stream delta and flood plain. The present
Tonawanda creek meanders northward across this plain into the
town, crossing the glacial stream courses, and then turns abruptly
west. A mile from the turn its altitude is 880 feet and in 2 or 3
miles further it reaches the Warren plane. It seems certainthat the
west-flowing glacial waters would have followed the same course
if it had been open to them. Evidently they did not, for the
present stream winds sharply in a narrow channel among morainal
knolls. Here seems to be a critical point in the relation of glacier
and lakes. The ice front rested here on Batavia when the con-
ditions that compelled westward flow of the glacial waters suddenly
ended, and the glacial waters were sent eastward toward the
Mohawk.

The large volume of water indicated by these capacious water-
ways seems beyond the possible supply of the Tonawanda valley
alone, and suggests that other territory further east also sent its
drainage westward through these channels; which suggestion is
found to be the truth, as will be explained.

*

32 NEW YORK STATE MUSEUM

Channels conveying tributary water from Oatka and Genesee valleys

The territory covered in this chapter is not now a part of the Erie ©
drainage area, but belongs to the Genesee river. During the time
of the ice recession, however, an extensive region to the east, possibly
including all the Finger Lakes district of central New York” was
drained westward past the ice front until the latter had receded to
Leroy and Batavia, at which time it appears that lower escape was
opened to the east, through Syracuse, and the direction of the
glacial drainage was reversed. ;

Plate 6 shows the channels between the Tonawanda, Oatka and
Genesee valleys. The series of channels lying between the Tona-
wanda and Oatka are not excelled in their general character by any
other series in the Erian drainage. The entire slope from the
parallel of Linden to that of Batavia, 9 miles, is quite denuded of
its drift, and the numerous strong channels are mostly in rock. They
show the work of a large volume of water for a relatively short time.

The highest group of these channels lies south of the Erie Railroad
at West Linden, at 1300 down to 1200 feet, and all in rock. The
intermediate set of channels covers a breadth of 24. miles between
the parallels of Bethany and East Bethany, the Lackawanna Rail-
road lying in the lowest member of the series, at 1000 feet.

On the north side of the Lackawanna channel at East Bethany
is a fine example of a glacial outwash sand plain. The sinuous line
of the ice contact shows conspicuously along the highway, on the
northeast side, in the abrupt, irregular border of the plain and the
accented morainal topography below the level of the sand plain.
A strong esker, followed by the crooked road leading north, is the
bed deposit of the feeding stream.

The lower series of channels are broad and somewhat indefinite
scourways, from 1000 to 920 feet. They seem to be in drift, and
were so low and nearly graded to their base level (either the shallow
waters south of Batavia or the Warren lake at Corfu) that they were
unable to deepen their beds. The later flow seems to have filled
or leveled up whatever valley depression once existed at Batavia.

‘At the time of this writing the full history of central New York drainage
hasnot beendeciphered. Inaformer writing [Geol. Soc. Am. Bul. 1899. 10:44]
the idea was stated that Lake Newberry, which occupied the Seneca, Cayuga
and Keuka valleys, was extinguished by westward escape into Lake Warren,
near Canandaigua. This is now thought to be wrong, for it appears that
Lake Warren did not enter central New York until subsequent to the time of
all the ice border drainage in western New York. It now seems probable
that the local waters adjacent to Seneca valley on the west were lowered into
the Newberry lake, and that the latter finally found escape westward. If this
is the correct interpretation then the Bethany-Batavia channels carried for
a time the entire glacial drainage of all the territory as far east as Syracuse.

GLACIAL WATERS IN THE LAKE ERIE BASIN 33

Between the Oatka and the Genesee valleys only two definite
west-leading channels have been mapped. The higher is a deep,
rock channel, at altitude of 1000 feet, with a northwest direction,
opening into the Oatka valley at Pearl Creek. This is the eastern
representative of the Linden and Bethany channels. The lower
channel is 6 miles north and is utilized by the Lackawanna Railroad,
with altitude of 940 feet. These two channels were the outlet of
the seventh stage of the Genesee glacial lakes, which were named
in a former publication the Warren Tributary lake.

The curving direction of these channels on the valley slope shows
clearly the lobation of the ice front projecting up the low ground of
_ the Genesee valley.

Here ends the too brief description of the Erian glacial drainage
channels. But study of the region shows still other channels heading
east of Leroy at 800 feet altitude, and northwest at 700 feet, which
lead to the east. These are the beginning of a remarkable series of
low level drainage channels extending east through Syracuse to the
Mohawk valley. Those beyond Syracuse have already been de-
scribed in former writings [see p. 7], and those between Leroy and
Syracuse will form the subject of a future article.

Leroy and Batavia stand at the critical altitude between the two
opposite directions of ice border drainage. During all the centuries
while the ice front was melting back obliquely from the south slope of
the Erie basin the ice border in central New York was also receding,
so that low eastward escape was soon to occur through Syracuse.
As long as the ice front, lying against high ground in the Syracuse
district, shut out the central New York waters from a low eastward
escape they all passed westward to Lakes Whittlesey and Warren,
as described. But while the ice was resting over Batavia [see p. 31]
the relations changed so as to permit lower eastward flow, even for
the Oatka valley, and the direction of the ice border drainage was
permanently reversed.

When the ice front passed north of Batavia the glacial waters on
the east were down to perhaps near 800 feet, and the Tonawanda
creek found a sinuous course through the moraine and entered
Lake Warren as a land stream.

LOCAL GLACIAL LAKES

The drainage channels described in the preceding pages were the
outlets for the glacier-dammed lakes held in the valley basins. It
would be the more logical order to describe the lakes before describ-
ing their outlets; but the reverse order has been followed because

34 NEW YORK STATE MUSEUM

the channels are existing features, and so much more abundant, —
widely distributed and conspicuous that they can be appreciated
better than the other evidences of the extinct and now invisible
lakes which produced them.

These glacial water bodies can be divided, somewhat arbitrarily,
into two classes, according to the direction of overflow. (1) The
earlier lakes which poured their outflow across the divide into
drainage outside the Erie basin. This class of lakes produced
the channels described briefly on pages 15-18. (2) The later local
lakes which found escape for their surplus waters past the ice front
and across the intervalley ridges, but wholly within the Erie basin.
These lakes, which often constituted tributary series, made the
hundreds of channels which have been briefly described in the
preceding pages.

With outlets to southern drainage

All the larger lakes of this class existed in territory which has
not yet been surveyed for the State topographic map; and as the
study of lakes and water levels requires particularly a knowledge
of altitudes which are now known in this territory only along a few
lines of railroads, the investigation is made under a disadvantage.
Without the topographic map the amount of labor required to
secure full data is out of all proportion to the value of the results,
and hence the subject is discussed here only in a general and pro-
visional way, and subject to future correction and amplification,
when the topographic sheets of Cattaraugus and Wyoming counties
are available. The map, plate 1, will show the general course of
the main water-parting between Erian and Alleganian waters ,and
the passes or cols across this line.

At the extreme west end of the State one or more small lakes may
have been held in the north-sloping valleys with outlets across the
divide to French Creek. Other examples of this class of lakes may
be located on plates 2, 3, by the outlet channels across the main
divide. The two larger ones occupied the highest portions of the
Canadaway and Walnut valleys.

All the other notable lakes of this class lie in either Cattaraugus
or Wyoming counties. The earliest primitive lakes must have been
along the southern side of the Cattaraugus valley, in the heads of
the valleys which incline northward. The lowest pass available
for each valley was compelled to carry some overflow for a time,
but possibly leaving little evidence of the flow. (The word ‘‘time”’
is used in a geologic sense and as relative, and may cover 1o years, or
100 years, Or 500 years, or even more. We have no way of estimat-

GLACIAL WATERS IN THE LAKE ERIE BASIN 35

ing the rate of recession of the ice front, which was doubtless very
variable.) As the ice front retreated northward the smaller primi-
tive lakes blended together and the higher passes of overflow were
abandoned for lower, until finally only one channel persisted in
each large basin. The early lakes in the eastern part of the Catta-
raugus basin overflowed to the Genesee glacial waters, and finally
out to either the Allegany or the Susquehanna drainage; while
those in the south side of the basin all overflowed to the Allegany.

The main branch of the Cattaraugus rises in Wyoming county in
the towns of Java, Arcade and Freedom and flows westward, being
joined above Gowanda by the south branch. In the eastern part
of the basin the lowest escape seems to have been at Machias, where
a large stream-cut valley occurs at altitude of 1646 feet, by the
Pennsylvania Railroad levels. The first of the larger lakes in the
Cattaraugus basin, which we may call the Machias stage, overflowed
for ages through this great outlet to Ischua creek and the Allegany
river.

With further recession of the ice front a lower escape was uncovered
a few miles south of Gowanda, by the south branch of the Catta-
raugus, described as the Persia outlet on page 17. The opening of
this outlet lowered the waters more than 300 feet and inaugurated
the second Cattaraugus lake, which we will call the Persia stage.
This level seems to have been held until lower escape was permitted
on the slope west of Gowanda in the vicinity of Perrysburg, as de-
scribed on page 22.

Throughout the Cattaraugus basin there will be found in the
higher valleys many small stretches of level silts or sands which are
delta fillings made by side streams pouring into the Cattaraugus
lakes. These may lie at various levels, but the stronger or more
extended fillings will be found to correlate with the Machias and
Persia stages, as these were stable for longer time. These deltas
should occur at about 1650 down to 1630 feet, and at about 1320
down to 1300 feet. Probably some of the villages in the basin have
their sites determined by these level areas of gravel or sand, and
these will most likely correspond to one or the other of the levels

noted above. The lower water levels at Gowanda belong with the
second class of glacial lakes [see p. 41].

Local lakes must have existed in the basins of the several parallel
creeks lying in Erie and Wyoming counties north of the Cattaraugus
basin, and now flowing northwest. We will not describe these
lakes, but will simply name them in succession from west to east,
as follows: In Erie county the New Oregon-Clarksburg lake occupied

36 NEW YORK STATE MUSEUM

the valley of the south branch of Eighteenmile creek; the Boston
lake, the main valley of Eighteenmile creek; the. Glenwood-
Colden lake, the valley of the west branch of Cazenovia creek; the
Protection-Holland lake, the valley of the east branch of Cazenovia
creek; the Java-Wales lake, the Buffalo creek valley.

In Wyoming county two valleys were occupied by high-level
glacial waters; the Cayuga and the Tonawanda. The col at the head
of the Cayuga valley leads over to the Tonawanda valley $ mile north
of Perry’s Crossing, through a. swamp, with altitude of about 1380
feet (aneroid)’.

The upper sections of these two valleys were consequently flooded
with a single lake, named the Varysburg-Johnsonburg lake after
the two villages in the Tonawanda valley, and which had its outlet
west of North Java leading over to the Java-Wales lake, already
mentioned [see p. 20].

The details of the lake phenomena and history will be found an
interesting study when the topographic maps are in hand.

With outlets past the ice front

The lakes of this class are the successors in each valley of those
just discussed, but their direction of overflow was essentially differ-
ent, and their distinct recognition is important to the full under-
standing of the history of the glacial waters. The existence of
these lakes has frequently been mentioned or implied in the descrip-.
tion of their outlet channels across the intervalley ridges.

As these lakes had a series of evanescent outlets across the declin-
ing ridges their levels were comparatively unstable, in which respect
they are quite unlike their predecessors of the former group. Another
difference is that these lakes were in series, one tributary to another,
but always to the westward.

The highest outlets have not been noted in all cases, and have not
been specially sought. They must always lie inferior to the head
waters outlet of the earlier lake. When the topographic maps are
at hand and altitudes are known it will be easy to locate the highest
escape of each lake with considerable accuracy in advance of actual
observation on the ground.

It is not now practicable to name all these lakes individually,
since they fell continuously through hundreds of feet vertically and

1In a former publication Glacial Waters in the Finger Lakes Region of
New York [Geol. Soc. Am. Bul. 10:33] this col was described as the early
outlet of the Tonawanda valley waters. This was an error, due to misin-
formation. Having no reliable map the writer accepted the statement that
the valley leading northeast from the swamp was the head of the Buffalo
creek valley, whereas it is the head of the Cayuga valley and leads far north-
ward.

GLACIAL WATERS IN THE LAKE ERIE BASIN 27)

tr

i
i.

contracted their areas until finally lost in either Whittlesey or

Warren. They are properly named after the village or some other
_ geographic feature in the lowest part of the lake bed.

Passing from the west the first lake of this class worthy of present
mention is that which was held in the Canadaway valley, south of
Fredonia, and already called the Shumla lake [p. 21]. This is a good
type of this class of lakes, and its description will apply, in a general
way, toall. The earlier lake had its outlet at the pass to southern
drainage through the present Cassadaga lakes and Lilydale and
Cassadaga villages. When the ice, resting against the slope south

_of Fredonia, was melted away from ground lower than the Cassadaga
outlet, and which had opening freely to the west, the second lake
was initiated. This highest channel to the west seems to have been

' at the three-corners, 3 miles west of Shumla and over 4 mile south

of the mouth of the Wheelers Gulf canyon. The Cassadaga col is
about 1320 feet altitude, and the westward escape is somewhat
under 1300 feet.

This second Shumla lake was not long stationary for the with-
drawal of the ice front on the sloping ground opened lower and still
lower outlets, and the vigorous streams cut the series of bluffs and
channels on the north-facing slope south of Fredonia. Not only was
the lake surface lowered and the area contracted but as the ice
barrier receded the lake followed. The lake thus migrated down
the valley, diminishing in depth and area until finally it was lost in
or blended with the invading Lake Whittlesey. The several channels
serving as outlets of the Shumla lake with the correlating deltas
have been described on pages 21, 22.

The next lake on the east was in the Walnut valley above Forest-
ville. Probably some delta fillings may be found along the slopes
which correlate with the stronger outlet channels across the slope
to the westward. The village of Forestville lies on a delta built in
the waning lake at its latest phase by the main creek, which had
followed the lake as the lake had followed the ice.

The lake next eastward and the largest of all the lakes of this
class in the Erie basin was the third phase of the Cattaraugus waters,
determined in its several levels by the series of channels winding
around the slope between Gowanda and Forestville. Two sets of
terraces or water levels are found in the lower part of the valley,
at Gowanda. The lower set was produced in the embayment of
Lakes Whittlesey and Warren. The upper set correlates with the
westward-leading channels. They are specially well developed
at Gowanda village, and were briefly described in the former writing
on this region.

38 NEW YORK STATE MUSEUM

The highest of the Gowanda levels is seen in a water-leveled plateau
some distance southeast of the village, with altitude about 1210,
or 100 feet lower than the Persia outlet (to Allegany flow for the
second stage waters). Immediately south of the village is a high
plateau terrace at 1032 feet, called the Studley level. The Broadway
level is a strong terrace south of the village at 972 feet. Below the
Broadway level is another terrace, named the John Brown level, at
883 feet, which corresponds precisely with the summit level of the
broad Asylum plateau, northwest of the village and west of Collins.
The high tower and water tank of the State Insane Asylum stands
on the 883 feet level. Shoos corners, on the north side of the plateau,
are on a broad terrace at 873 feet; while a lower plain at 857 to 852
feet forms the State farm and the site of Collins village. With the
help of Mr B. W. Law these water planes were measured for altitude
in 1900 without any knowledge of their correlation beyond the idea
that the determining outlets were on the high ground to the west.
During the summer of 1902 the slope between Perrysburg and Forest-
ville was examined and the stream channels mapped entirely inde-
pendently of any other features. Indeed the correlation of the
channels with the Gowanda terraces was not made until the time
of this writing. The relationship can now be expressed in the
following table:

GOWANDA PLANES OUTLETS
Highest plateau, 1210 feet Highest well developed channels
across high ground west of Perrys-
burg :

Minor scourways at various
levels above and below 1100 feet
Studley plateau, 1032 feet Strong channels at Smiths Mills
station, and east, at 1020 feet
Strong cut terraces and bluffs
Broadway level, 972 feet north of West Perrysburg and
: around to Forestville, at 980 down
to 920+ feet
Strong channels at Smiths Mills
Asylum plateau, 883, 873 feet and east and west, at goo, 880 feet

and lower
Lowest channels west of Smiths
Collins plain, 855 feet —. Mills and west of Forestville, at
about 860 feet and declining
Fourmile level, 820 feet and Lake Whittlesey, 840 + feet

declining west

GLACIAL WATERS IN THE LAKE ERIE BASIN 39

The figures for the outlets are taken from the map contours and are

not precise. Accurate measurements would probably show closer

correspondence than this tabulation. When we realize the con-
siderable variation in altitude of the water-leveled plains with
reference to the water surface, and the fact that the lake waters were
slowly drained down through all the levels from the highest to the
lowest, the above correspondence is very striking and conclusive.
It shows a harmony of facts indicating that the theory is sound.

Passing east from the Cattaraugus we shall find that the same
series of parallel valleys which held lakes of the earlier class [see
Pp. 35] also held lakes of this group, and with lowering surfaces as
shown by the numerous channels already described as lying across
the ground between the valleys. It seems unnecessary to recapitu-
late the lakes by the former names; and it is not desirable to give
distinct names merely in recognition of changing outlets and different
levels until we can describe them with greater detail and precision
than is possible without the topographic sheets. In each valley a
good observer can probably find sufficient lake and stream phenom-
ena to yield an interesting history when translated by competent
study and correlation.

In the Tonawanda valley the Attica lake was the successor of the
Varysburg-Johnsonburg lake. The overflow channels of this water
have already been described as the numerous strong channels lying in
the broad belt north and south of Darien and Darien Center. Delta
plains and terraces should occur along the sides of the valley at
various levels. It would seem that they should be stronger at
about goo to 1050 feet, or correlating with the stronger overflow
in the region of the Lackawanna and the Erie Railroads; but the
conspicuous delta plain of the State Asylum farm at Varysburg, at
1200 feet, must correlate with some other outlet. The delta east
of Alexander, at 950 to 920 feet, was built when the waters had outlet
along the line of the Lackawanna Railroad. When the outflow
was near Batavia the lake was too shallow and restricted to reach up
the valley beyond Attica.

The theoretic succession of waters in the Tonawanda valley may
be outlined as follows:

t North Java lake. The outlet not determined, but at about

1600 feet.

2 Varysburg-Johnsonburg lake. Outlet west of North Java,
GLO at 1CeL.

3 Same lake, second stage. Flooding Humphrey Hollow (Cayuga

valley). Outlet near North Sheldon, at 1500 to 1400.

40 NEW YORK STATE MUSEUM

4 Same lake, third stage. Outlet into Humphrey Hollow lake by
the swamp col at Perry’s Crossing station, 1380+ feet.
5 Same lake, fourth stage. Direct outlet past the ice border
south of Bennington, under 1380.
6 Attica waters, many stages. Outlets between Darien and
Batavia.

In valleys east of the Tonawanda creek

The local lakes mentioned thus far were in valleys of the present
Erie drainage. But during the glacial epoch and the episode which
we are studying the valleys far to the eastward were tributary to the
Erian waters, as already noted [p. 32].

The eastward extent of the territory which was drained by the
Bethany-Batavia channels is not yet certain, but at its maximum
it may have reached nearly to Syracuse. One determining element
in the problem is the plane of the Newberry waters which had their
outlet south, through Horseheads and Elmira, at the present alti-
tude of goo feet. |The Newberry plane rises toward the north, like
all of the glacial lake levels, and on the parallel of Batavia should have
an altitude of about 975, or 100 feet over the Warren plane. With
present partial knowledge of the trend of the ice front in the Finger
Lakes district it seems probable that this front lay far enough to the
north to allow free passage westward to the Newberry waters during
the life of the Batavia channels. If this were the fact then the
channels lying north of East Bethany, or from 975 to 950 feet,
carried Newberry waters and diverted the flow from the south-
leading Horseheads outlet, and all the territory as far east as Owasco
and Skaneateles valleys was drained through the Batavia channels.
Whether the above suggestion is true or not, it seems certain that
the valleys of Oatka, Genesee, Conesus, Hemlock and Honeoye
were tributary to Erian waters.

The Batavia channels might seem incapacious for the volume of
water that would be contributed by so large a drainage area and
from so long a frontage of melting glacier. But the scourways were
not cut deep for the reason that they were already so low relative
to their baselevel, the Warren plane. From Batavia to the Warren
plane west of Corfu is about 12 miles, with a fall of about 30 feet.
The Batavia plane and the buried moraine south and southwest
show the effects of a large volume of water with a sluggish flow.

The earliest lake in the Oatka valley, called the Warsaw lake, had
its outlet southward through Silver Springs at altitude of about
1400 feet. The channels above described, at Linden and the Beth-

ap ee i et eel ee

tr

GLACIAL WATERS IN THE LAKE ERIE BASIN 4I

anys, were the westward outlets of a lower lake, with levels falling
from about 1300 feet down to tooo feet, which we will call the
Wyoming-Pavilion lake. ;

The full history of the waters in the Oatka and Genesee valleys
belongs to another paper which should treat specially of the Genesee
and central New York valleys.

GREATER GLACIAL LAKES
General statement

The evidences of standing water at high levels in the Huron-Erie
basin were recognized in the early occupation of the territory, and
many geologists have participated in the investigation, among
whom should be mentioned N. H. Winchell, J. S. Newberry, G. K.
Gilbert, J. W. Spencer, C. R. Dryer, and specially Frank Leverett
and F. B. Taylor. The elaborate monograph by Leverett, already
noted, is the latest comprehensive treatise on the subject, and its
pages 711-55 give a good account of the lake history and records,
with excellent maps. Recently Taylor has worked out in Michigan
the history of the greater lakes in correlation with the different
positions of the oscillating ice front.

For several years three vast glacial lakes, successively lower in
altitude, have been recognized in the Huron-Erie basin. These
have been named lakes Maumee, Whittlesey and Warren. Recently
Taylor announces another lake level, ‘“‘Arkona”’ representing a
stage between the Maumee and the SHEDS), but lower than the
latter.

Lake Maumee

This earliest member of the series of great lakes in the Erie basin
named by Dryer in 1888, did not extend into New York. It was
initiated when the ice front retreated from the head of the Maumee
valley at Fort Wayne, Ind., and the primitive and principal outlet
was at Fort Wayne over to the Wabash-Mississippi. As the convex
ice front receded northeastward the lake followed it until the southern
branch of the lake, creeping along the glacier margin, reached as far
as Girard, Pa. At the same time the western branch pushed along
the ice margin in Michigan and found another and somewhat lower
escape at Imlay across the ‘‘Thumb” of Michigan (the point of land
between the south end of Lake Huron and Saginaw bay) over to the
glacial lake Saginaw (occupying the Saginaw valley) which poured
its waters into the glacial Lake Chicago (occupying we Michigan
valley) with ultimate flow to the Mississippi.

42 NEW YORK STATE MUSEUM

Further recession of the ice front on the Michigan “Thumb”
extinguished Lake Maumee, by opening an escape for the ice-1m-
prisoned waters at a lower level. It has been supposed that the -
successor of Maumee was the next lower of the lakes which have
left their shore inscriptions in the region, that is, Lake Whittlesey.
But Taylor has recently found that the relation of shore lines and
moraines indicates that the ice front receded from the Maumee level
directly to a level below the Whittlesey and opened free passage for
the waters to Lake Saginaw. This level of the waters in the Huron-
Erie basin is thought to have persisted for a long time and to have
formed the extensive beaches in Michigan and eastward, known
as Arkona (named by Spencer).

At length a readvance of the ice in Michigan closed the Arkona
outlet and forced the overflow to a higher level, farther south, on
the thumb of Michigan, at Ubley. The beaches correlating with
the Ubley outlet have long been known as the Belmore (named by
N. H. Winchell from a town in Ohio) and the waters arye —
named by Taylor Lake Whittlesey.

The fall of the glacial waters from the Maumee down to the Arkona
level with the subsequent rise to the Whittlesey level the writer
believes to have occurred while these waters were yet excluded
from New York. The facts and argument bearing on the above
history will be found on pages 64-75. However, the continued
recession of the Erian ice lobe during the life of Lake Whittlesey
allowed these waters to push far into New York. In the State of
New York we have, therefore, to deal only with Whittlesey and
lower waters.

Lake Whittlesey

This water body, named by Taylor in 1897, was the successor to
Lakes Maumee and Arkona in the Huron-Erie basin. Its outlet
was at Ubley on the Michigan ‘‘Thumb,”’ in a reentrant angle of the
ice front. The overflow was contributed to the glacial lake Sagi-
naw, in the valley of that name, which in turn had its outlet across
Michigan by the Grand River valley to Lake Chicago. The strong
shore line named by Winchell in 1872 the ‘‘Belmore,” after the
town in Ohio, is the beach of this lake. The Whittlesey beach
extends into New York with strong development but weakens
beyond Gowanda and disappears between East Aurora and Alden
near the village of Marilla.

The Whittlesey shore has suffered deformation in common with all -
the beaches in the Erie basin, and rises from an altitude of 784 feet
above ocean at State Line (taking the elevation of the track of the

GLACIAL WATERS IN THE LAKE ERIE BASIN 43

Lake Shore & Michigan Southern Railroad at 787 feet) to 905 or g10
feet near Marilla.

The detailed description of this shore line will follow on later
pages.

Lake Whittlesey came to its extinction by the recession of the ice
front on the “Thumb” of Michigan which finally allowed the waters
to fall to the level of, and to blend with, Lake Saginaw, the extended
waters being called Lake Warren.

Lake Warren

This name is applied to the wide extended glacial waters that in
the Huron-Erie-Ontario basin succeeded Lake Whittlesey, with its
surface about 45 feet lower. While the ice margin was lying south
of Alden, N. Y., its western continuation on the “‘Thumb”’ of Michi-
gan receded from its position facing the Ubley channel, and the Whit-
tlesey waters found lower escape and were finally blended with Lake
Saginaw. Lake Warren was, therefore, only the far-extended
Lake Saginaw, with outlet by the Grand River valley into the glacial
Lake Chicago near Grand Rapids.

The Warren waters found their way eastward past the slowly
receding ice front into central New York, and the great lake came
to its extinction by the opening of new and lower outlets eastward to
the Mohawk-Hudson in the region of Syracuse. The map in the
22d annual Report of the State Geologist, plate 1, shows the full
extent of the Warren waters in New York. They formed only a
narrow belt of open water south of the glacier margin, with
numerous prolongations up the valleys of the Finger Lakes.

Unlike the Whittlesey shore, which is a unit and definite, the
Warren shore phenomena about the Erie basin are complex, includ-
ing usually a series of bars, ranging from 4o or 45 feet down to 70
feet below the Whittlesey. This multiplicity of the sand and gravel
ridges has been regarded as the product of distinct levels of the
lake waters, and in the writings of Leverett and Taylor the upper
bars have been called Arkona, and the lower ones Forest (named by
Spencer after a town in Ontario, Can.). The present writer has a
different view as to the origin of the shore features, but the relation-
ship and genesis of these beaches will be discussed later, after the

detailed description.
Lake Dana

Lake Warren ended by the opening of channels of escape east-
ward to the Mohawk-Hudson. The falling waters with easterly
outflow might be distinguished as sub-Warren or hypo-Warren,

44 NEW YORK STATE MUSEUM

but since they were tending toward the Lake Iroquois level, having
the outlet at Rome to the Mohawk valley, they have more properly
been called hyper-Iroquois.

From the Warren to the Iroquois plane the lake waters fell
through 440 feet of vertical distance (Warren level in central New
York about 880, Iroquois about 440), and long pauses must have
occurred during the lowering of the great volume of water and the
cutting of the huge canyons and cataract cliffs in the Syracuse
region which rival those of the present Niagara. Only one of these
stages has been recognized, namely, that which produced the strong
beach first discovered in the Seneca valley and named the Geneva
beach, the producing waters being called Lake Dana.

The altitude of Lake Dana is 700 feet, or 180 feet under the
Warren plane. Its outlet is believed to have been the capacious
channel leading east from Marcellus, as that is the only Sasol
channel with the proper hight.

Numerous and indubitable evidences of this water surface have
been found in wave-cut notches and spits of gravel on the hills as
far west as Buffalo. Theoretically it should extend westward over

the same general area as the Warren, and many evidences of standing

water have been found in the Erie district at the Dana level, declin-
ing westward in accord with all the water planes, but no con-
tinuous beaches are found as the waters were too transient to do
much work under unfavorable conditions. Lying 180 feet under.
the Warren plane the Dana plane passes under Lake Erie in the
neighborhood of Westfield. Eastward, strong bars have been found
at Fayette, between Seneca and Cayuga lakes.

SHORE LINES OF THE GREATER LAKES

General description of the beaches

The general relation of the ancient lake beaches to the present
geography can be more clearly understood by examination of the
maps than by verbal description alone. By reference to the maps
[pl. 2-6] it will be seen that the several beaches lie in a belt which
has, in general, a straight course across the entire area, with north-
east by southwest direction from State Line to Indian Falls, a
distance of nearly 90 miles. The chief exception to the above
statement is the embayment at the Cattaraugus, which however
affects only the higher beaches. It will also be seen that in the
stretch from State Line to Silver Creek, about 38 miles, the beaches
lie close together and parallel with each other and with the present
shore of Lake Erie, which is only 1 to 3 milesaway. At the embay-

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WAVE-WORK OF LAKE ONTARIO

The primitive shoreline passed around all the bays.
embankments across all the bays on the south shore of the lake.

wholly built by the lake waters.

Wave-work has eaten back the headlands and constructed

The bar connecting Lake Bluff with Charles Point is

Compare plates 15,16. (These three illustrations from an existing lake show the forma-

tion of cliffs and bars on the ancient lake shores. )

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GLACIAL WATERS IN THE LAKE ERIE BASIN 45

ment or indentation in the higher ground forming the Cattaraugus
valley the higher beaches swing landward, toward the southeast,
nearly to Gowanda, or about to miles. Beyond this break, the
belt of beaches continues its northeast course, but the beaches
lose their continuity and parallelism. From the Cattaraugus to
Eden Valley the higher beach, the Whittlesey, can be continuously
traced by cliffs or bars, while the lower shore phenomena, the
Warren, are discontinuous though strong, and distributed over a
belt 2 or 3 miles wide. From Eden Valley to Indian Falls, on the
contrary, the Warren beaches become more continuous and direct,
while the Whittlesey beach, lying across ridges and valleys, is
immature, broken and irregular and weakens and finally disappears
near Marilla.

Throughout its whole extent in New York the Whittlesey beach
is characterized by simplicity and unity. When marked by wave-
built bars or embankments of sand and gravel it is single and definite
and fairly strong excepting of course toward its extinction east
of Buffalo. In this respect the Whittlesey and Warren are very
different. The Warren shore phenomena are complex, being only
exceptionally a single ridge of gravel. Usually the Warren forms
several ridges, variable in strength and altitude. This complexity
of the Warren shore will be discussed ina later chapter after the
phenomena have been described in more detail.

In the Huron and western Erie basins the prevailing eomplemita
of the Warren shore phenomena and frequent pronounced du-
plicity gave occasion for distinct names and for the belief in two
distinct lake levels. The higher of the more persistent ridges was
called ‘““Arkona”’ and the lower “‘Forest,’’ names given by J. W.
Spencer to beaches in Ontario, Can. Throughout the district
in New York described in this paper two bars or two series of bars
may frequently be recognized, and the names Arkona and Forest
have been used by Leverett in the description of this region.
While convenient for use in study and discussion the names are
inappropriate for final or permanent designation of the New York
beaches since the types are far away in another province, implying
two lake levels which are not yet proven, and are not descriptive or
suggestive of the lake which produced them. The appropriate
naming is to designate the beaches fractionally or locally by some
geographic feature, usually a village on the bar, and to
tefer to the beaches in the comprehensive way as the higher or
superior Warren and the lower or inferior Warren. These names
will be noncommittal on the question of two distinct lake levels.

40 NEW YORK STATE MUSEUM

and can readily give way to any more distinctive names if needed in
the future. ;

To the readers who are not familiar with shore phenomena a
few words of description will be helpful, but observation in the field
is the best teacher. The shore work done by lakes and seas is
effected by the waves beating against the shore and by the currents
running more or less parallel with it. The waves undercut
the projecting points or saliences while the currents seize the
resulting detritus and push it along the shore or into deeper water.
The final result of this work is to pare away minor projections and
to build ridges of sand or gravel across the narrower bays or re-
entrants, thus straightening or smoothing a shore line which
primitively may have been very irregular. This geologic process
is well illustrated along the shores of living waters and plates 14-16
clearly show the work on the Ontario shore at Sodus Bay.

When the work of waves and currents along a stretch of shore
has accomplished all that is possible in the way of straightening the
latter the beach is said to be “‘mature.’’ Some geographers do not
regard the shore as mature until all the lagoons behind the bars
are filled by detritus from land wash or by vegetal accumulation,
thus making a continuous mainland.

The shore of Lake Warren is comparatively straight and mature
as far east as Crittenden, beyond which point the beaches indicate
very much less work of the waters. The Whittlesey beach 1s fairly
developed to the Cattaraugus embayment, beyond which the
wave work diminishes.

Detailed description of Whittlesey and Warren beaches

As the direction of the beaches, highways and railroads are nearly
northeast and southwest, parallel with the Erie shore, the constant
reference to compass directions is verbally awkward. It will be
more convenient in the description to speak of the directions
alongshore as east and west, and the direction at right angles to
this as lakeward and landward.

The figures given for altitude are usually by aneroid unless
otherwise stated, but these are fairly reliable as the instrument
was frequently checked by the railroad levels and all doubtful
figures have been thrown out.

State Line to Westfield. At the New York-Pennsylvania bound-
ary all the beaches lie below (or lakeward of) the railroads, in which
respect the locality is unique in New York. At State Line station
the Whittlesey (Belmore) beach is a ridge or terrace supporting

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GLACIAL WATERS IN THE LAKE ERIE BASIN 47

the station of the Lake Shore and Michigan Southern Railway,
which is given as 787 feet. The beach altitude is taken as three
feet lower, or 784 feet. The conspicuous ridge east of the station,
lying between the two railroads, which suggests a bar in form,
is a morainal ridge and the west front of the Escarpment moraine.
The Whittlesey waters laved the moraine in all this section.

West of the railroad station the Whittlesey beach swings over to
the highway, carrying State Line village, and is followed by the

Sketch of bars on delta of Twentymile creek at State Line

Fig. 2

48 NEW YORK STATE MUSEUM

highway, into Pennsylvania. The relation of the geographic fea- —
tures is roughly indicated in the sketch, figure 2. We findhere ©
a characteristic development of wave-built bars ona delta, the
' delta of Twentymile creek. The horizontal spacing in the sketch ~
is not accurate, being only estimated. The vertical spacing or
altitudes are by aneroid and hand level and fairly reliable. The
total vertical spacing of the Warren bars is about 50 feet. The
interval of 45 feet between the Whittlesey and the upper Warren,
and 25 feet between the upper and lower Warren is a fair example
of the prevailing relation as far as the Whittlesey extends. The
duality of the Warren series is unusually well expressed, and is
possibly somewhat overemphasized in the sketch. On a strong
delta bars may form rapidly, and the multiplicity of bars with
some of inferior level, makes the delta. bars, when taken alone,
unsafe criteria for determination of the lake levels.

On the roads 14 miles eastward from State Line the Whittlesey
bar lies between the railroads in excellent form at the altitude
(aneroid) of 782 feet. The higher Warren carries the ‘‘Ridge Road”
at 734 feet, while the lower Warren lies lakeward with altitude 715
feet. The highway follows the higher Warren east for 4 mile at
which point the lower ridge unites with the higher, and on through
Ripley village there is only one Warren beach, followed by the
main street, with an altitude of 730 feet, and 60 to 70 feet under
the Whittlesey. Southwest of Ripley 14 miles the Whittlesey
beach is crossed by the Chicago and St Louis (Nickel Plate) Rail-
road, and from this point eastward throughout its whole extent in
New York it lies above or landward of the railroads. This is the
only locality in New York where the traveler on the railroadsis able
to plainly see the Whittlesey beach, although a trained eye may
detect the wave-cut slope between here and Brocton, lying above
the Warren bars.

South of Ripley, lying under a highway, the Whittlesey beach
is a broad, low ridge against the morainal slope. Nearer the
village the beach falls below the road and farther east it carries
the cemetery. The main street of Ripley at the east end of the
village lies on the lower Warren, about 15 feet under the Lake
Shore tracks, which are given as 749 feet, making the lower beach
734 feet. The Whittlesey lies about on the 800 contour of the
topographic sheet. The railroads lie along the higher Warren
which they have largely cut away.

In the stretch of 8 miles from Ripley to Westfield the Whittlesey
beach lies against the steep morainal slope and is often weak and

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discontinuous. In some places it has left no trace except a smooth-
ing of the slope, one such point being on the road leading landward
over a mile southwest of Forsyth. From Ripley to Forsyth it
lies about 4 to 4 mile landward of the railroads.

The highway between Ripley and Forsyth follows the lower
Warren, while the railroads occupy the position of the upper Warren
which they have dissected or leveled. One mile east of Ripley
the altitudes are: Whittlesey 796, higher Warren 761, lower War-
ren 730 feet. One half mile west of Forsyth the Warren is repre-
sented only by the lower bar, under the highway, 735 feet, while
at the station this is distinct under the depot at 730, and the
higher Warren lies above the railroad.

East of Forsyth the railroads lie lakeward of the beaches and
thence eastward lie on the floor of the lakes while the highway
follows the Warren beach. One half mile east of Forsyth the bars
all have good development, specially the Whittlesey. On the road
leading landward the following altitudes were taken: Whittlesey
792, higher Warren 760, lower Warren two bars 744, 730 feet.

East of Forsyth 14 miles and beyond four-corners only one ridge
of Warren is shown. The Whittlesey is here a heavy bar of fine
gravel and the interval between this and the Warren is 65 to 70
feet. About 2 miles southwest of Westfield a new road has been
made, leading south, and on this road a small bar occurs inter-
mediate between the Whittlesey and Warren. The intervals
are about 25 and 16 feet, or 41 feet between Whittlesey and Warren.

About ‘1 mile west of Westfield, by the three corners, the Warren
bars, all lying north of the highway, show fine development and
multiplicity. There are four strong, close set ridges with vertical
intervals in descending order of 11, 10 and 6 feet by hand level,
giving a total range of 27 feet.

Approaching Westfield the beaches swing around up the creek, the
upper Warren falling into line with the bold ridge of the Whittlesey.
The inferior Warren is a weak bar 4 mile north of the higher bar,
and the beach altitudes here are 725, 745, 795 feet.

Westfield village lies on a delta of Chautauqua creek, bounded
landward by the Whittlesey beach. The main street cuts through
the higher Warren ridge, the break occurring at the high school.
Bast of the school building and public square the superior Warren
forms on the southeast side of the street, the strong ridge occupied
by residences and the cemetery. The crest of this ridge is 5 feet
over the United States Geological Survey bench mark (on the
school building), making the altitude of the beach 753 (748 plus s)

GLACIAL WATERS IN THE LAKE ERIE BASIN 49

50 NEW YORK STATE MUSEUM

feet. Several lower Warren ridges occur on the delta plain, as
mapped in figure 3. The altitudes here are: Whittlesey 795,
higher Warren (precise) 753, lower Warren 730, 725, and a still
lower bar at 718 feet.

Westfield to Portland. In this stretch of 7 miles the two shore
lines and the railroads hold a fair parallelism. The Warren bars
lie along the highway about 4 mile from the railroads, while the
Whittlesey lies about # mile farther landward. South of Westfield
and for 3 miles northeast the Whittlesey is a handsome ridge

Plate 17

highway.

ge carries a

The rid

Looking south from the lake bottom.

Warren beach, 1 mile west of Ripley.

a

GLACIAL WATERS IN THE LAKE ERIE BASIN 5t

[see pl. 18] pursuing a direct course and presenting a bold lakeward
slope. The 800 foot contour of the topographic sheet should lie
along the face of this conspicuous ridge.

From Westfield to West Portland church, 34 miles, the highway is
a direct line and lies on the lower Warren beaches. As seen from
the road the beach is a broad, undulating ridge with a steep frontal
or lakeward slope, facing the smooth plain of the ancient lake
bottom. For 2 miles from Westfield the superior Warren is not
prominent but represented by low, parallel bars somewhat higher
than the highway. Gradually, however, the higher Warren
strengthens and toward the West Portland corners it becomes a
heavy gravel ridge about 38 feet higher than the lower Warren.
This is an interesting locality for the study of these water levels.
At the forks of the road the highway leading to Portland and Broc-
ton rises quickly from the lower to the higher Warren ridge. The
brick church stands on the upper Warren ridge, which beyond this
point is a gravel plain nearly a mile wide, extending landward to
the Whittlesey. beach. Along the road the surface of the plain is
a series of smooth ridges or swells, specially toward Portland and
along the edge of the plain, the latter forming a steep cliff 35 to 40
feet high, and about 4+ mile from the highway. The lower Warren
ridge lies below the cliff, which seems to have been eroded by the
later Warren waves, as shown in plate 19. This broad gravel plain
is the delta built in the Whittlesey and lowering waters from the
detritus brought down by the glacial drainage channel south of
Portland [see p. 21]. The large vertical interval between the
Warren bars contrasts strongly with most other localities. On the
north and south Townline road west of the brick church the lower
Warren is about 25 feet under the upper Warren, and the Whit-
tlesey is toward 50 feet higher. At the brick church the Whittlesey
lies 40 to 45 feet over the upper Warren, which is 38 feet over the
lower Warren, represented here by a single bar below the abrupt
cliff.

On first sight the large interval between the Warren bars suggests
two lake levels about 4o feet apart. But this relation is not con-
firmed at other localities. The relation here is exceptional and the
product of special local conditions. The isolated lower bar may
be regarded as inferior Warren, either an offshore construction or
else built in the falling waters. It is comparable to the inferior
bars often found on heavy deltas.

In the section of the West Portland corners and brick church the
Whittlesey beach is a cliff for about 14 miles, but eastward it be-

52 NEW YORK STATE MUSEUM

comes a strong gravel ridge under the highway which utilizes the
ridge for 9 miles, or to within 2 miles of Fredonia. Southeast
and south of Portland the Whittlesey and its highway lie on the
delta plain, but eastward the beach forms the north bank of the
conspicuous river channel already described on pages 20, 21. This
locality near Portland, with the glacial river channel, the delta
plain with wave-built bars on top and its wave-eroded front, all
lying at or just below the Whittlesey level, makes it one of great
interest and critical importance.

Portland to Fredonia. From 2 miles southwest of Portland to r4
miles southwest of Fredonia, a distance of at least 9 miles, the
Whittlesey beach is followed by the “Ridge road,” and is roughly
parallel with the Warren shore and its highway. South of Brocton
the two ridges are nearly a mile apart, while 2 miles east and south-
west of Lamberton they are only 4 mile apart, these being the
extremes of horizontal spacing in this section. The course of the

Whittlesey shore is more indirect than that of the Warren as it

bends to the irregularities of the higher ground, while the Warren
lies on the Whittlesey bottom and delta fillings. In all its course
from Portland to Fredonia the Whittlesey beach faces, or lies lake-
ward of stream-cut bluffs or river channels eroded by glacial
drainage. For most of the distance it is a definite ridge of gravel,
[see pl. 20], but in a few places it is a wave-cut cliff. One such cliff
occurs south of Brocton, and others south of Lamberton.

The Warren shore is unusually varied in form and character
between Portland and Fredonia. Portland lies on the higher and
broader of several bars. Halfway between Portland and Brocton
there are three bars with intervals, in descending order, of 35 and
20 feet. Brocton village lies below the Warren beach. One half
mile east of the village the highway rises on to the beach, which
for over a mile is a low bar facing a bold, wave-cut cliff cut in the
delta front. Nearing Lamberton the beach is lost in an eroded
embayment in the delta. For 4 mile east of Lamberton the road
is on the single Warren ridge, but for the next 14 miles the beach is
a broad gravel plain, with several ridges, and an abrupt border 4
mile north of the road as shown in plate 21. This plain is another
delta plateau, leveled by Warren waves, but probably accumu-
lated in Whittlesey waters from glacial drainage.

Toward Fredonia the road rises slightly above the Warren level,
and is on till. The beach lies on an abrupt but eroded delta front 4
to 4 mile lakeward of the road. No lower Warren bar is dis-
tinguished in this section unless it is represented by a short spit

Plate 18

Looking southeast from the lake bottom.

Whittlesey beach, 14 miles east of Westfield.

: ~

_ GLACIAL WATERS IN THE LAKE ERIE BASIN 53

close to the road on the south side of the creek. The several
altitudes west of Fredonia are estimated as follows: Whittlesey 813,
higher Warren 768, lower Warren 743, lake bottom 720 feet.

Fredonia to Walnut and Silver creeks. Along this stretch of ro
miles the shore features are excellently developed, continuous,
straight, and for much of the distance the Warren beach is distinctly
double. Not much verbal explanation is needed as the phe-
nomena are clearly shown on the map. The road leading northeast
from Fredonia lies on the higher Warren ridge for 34 miles, then
follows the lower bars for nearly 7 miles to Walnut creek. At the
railroad station in Fredonia the higher Warren ridge is about 8
feet over the railroad station which is given as 762 feet. Using
this as the datum the beaches near the village are: Whittlesey
820, higher Warren 770, lower Warren 750 feet. The cemetery is
on the lower Warren.

Two miles east by north from Fredonia a conspicuous mound or
cone of till stands in the Whittlesey beach and has been described
on page 13.

Four miles from Fredonia the higher Warren loses its distinctive
character and for a mile breaks up into low, disconnected bars, and
afterward for 3 miles is practically unrepresented, the highway
following the lower Warren all the way to Walnut creek. At
Sheridan Station on the Erie Railroad the Warren consists of two
low, broad sand bars between which lies the highway. Using the
map figure of 758 feet for the west road crossing of the railroad as
the datum, the altitudes at Sheridan are: Whittlesey bar 825,
higher Warren (cemetery) 766, lower Warren (north of road)
755 feet. This gives vertical intervals of 59 and 11 feet. Former
measurement made the intervals 60 and 1o feet. It will be found
that 8 miles east the same intervals occur. Northeast of Sheridan
for over a mile only the lower Warren ridge can be seen in the open
ground, but at the south-leading road 2 miles from Sheridan the
upper Warren reappears, and the altitudes are: Whittlesey 825,
upper Warren 785, lower Warren 755, the vertical intervals being
40 and 30 feet. From this point to Walnut creek, 1? miles, the
higher Warren is a conspicuous, strong ridge lying + mile landward
of the highway with a steady vertical interval of 30 feet above the
lower Warren.

Approaching Walnut creek the Whittlesey beach, which all the
way from Sheridan has been diverging from the Warren, acquires
an east and west direction, and at the creek lies on the front of
the Forestville delta, 2 miles south of the lower Warren, the latter
keeping to its northeast course. ee,

54 NEW YORK STATE MUSEUM

Hanover Center (Silver Creek) to Gowanda. In this section and
the next one the Whittlesey beach swings far inland and all the
phenomena are complicated.

On the meridian of Walnut and Silver onedlce and Forestville the
beaches lie on a delta, accumulated partly by glacial drainage and
partly by the two existing creeks, in the successive lake waters.
The Whittlesey beach retains its simplicity but the Warren bars
are multiple. Between the two creeks the Whittlesey is a straight
ridge 14 miles long with northeast course. East of Silver creek
for 3 miles it is mostly a cut cliff on the face of the moraine. From
an angle of the Indian Reservation (1? miles northeast of Smiths
Mills) it is followed by the highway, chiefly as a ridge, with a trend
south of east for 24 miles; then it leaves the road and swinging
around to the southeast follows along the south side of the Catta-
raugus valley, mainly as a gravel ridge, for a distance of about 5
miles, or to within 2 miles of Gowanda. Above Gowanda the
narrow Cattaraugus valley is a postglacial ravine and the old
valley is blocked with drift, whence it would seem that the Whit-
tlesey waters did not reach beyond the village, although the level
would today extend far up the gorge valley. The altitude of the
beach south of the Cattaraugus creek is 840 feet, according to the
map contours.

Between the Walnut and Silver creeks along the north and south
road the Warren shore is represented by at least four ridges, of
which the two extremes correspond to the two strong ridges west
of Walnut creek. The vertical interval is 25 feet. At Hanover
Center and eastward there are several bars, the village corners
lying on the higher Warren, which is followed by the road north-
east for 14 miles. Farther east the road, about a mile long and
connecting two roads, lies above fragmental bars of the higher
Warren. North of the east terminus of this road and on the north
and south road, in the reentrant right angle of the Indian Reserva-
tion are two clean-cut gravel ridges with smooth clay soil inter-
spaces. These bars are beyond the limits of any delta, on a clay
slope, about + mile apart, and with vertical interval oF about 13
feet.

Eastward from the point noted above the lower Warren beach
lies along the top of the bluff, south of the Cattaraugus creek in the
Indian Reservation; while the higher Warren bars lie at the angle
of the road in the west limits of the Reservation and continue
east along the 800 foot contour. The bars have not been contin-
uously traced in the Reservation as the ground is in timber and with

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GLACIAL WATERS IN THE LAKE ERIE BASIN 55

few roads, but the higher Warren lies about halfway between the
lower Warren, on the top of the river bluff, and the Whittlesey a
mile south. On the north and south road west of Little Indian
ereek the altitudes are: Whittlesey 840, upper Warren 790, lower

Warren 770 feet.

The village of Versailles stands on the Warren terraces and the
shore line of Lake Warren crosses the Cattaraugus valley a short
distance above the village.

Gowanda to North Collins. The Whittlesey shore line is some-
what irregular and broken throughout the rest of its course in New
York, and fades out toward Marilla. The lake reached up the old
Cattaraugus valley as far as Gowanda, and doubtless some rem-
nants of its delta may be found about the village. The Erie Rail-
road station is given as 773 feet, or about 60 or 65 feet under the
Whittlesey plane. The extensive sublacustrine delta plain, locally
known as the “Four Mile level,’ will be described later under
deltas. The super-Whittlesey levels about Gowanda, formed by
the third stage of Cattaraugus waters, have been described under
local glacial lakes [p. 38].

North of Gowanda the Whittlesey shore is a cut cliff along the
west side of the State Asylum plateau, facing the Four Mile level
which was the lake bottom. The shore line swings around the north
point of the plateau and forms a bay north of Collins station. In
the return curve it crosses the Collins-Lawtons road about 50 rods
north of the residence of Mr B. W. Law, which stands on a broad
spit lobe. The altitude here is $39 feet, taking Collins station as 861.
After crossing to west of four-corners and then curving sharply up
the valley of a branch of Clear creek the beach returns to the east
side of the road leading to Lawtons, and for 3 miles it lies along the
east side of the road in the form of weak bars and cliffs. At the
Shirley road it makes a sharp curve to west of the corners around a
point of delta and then runs parallel with the railroad through
the east edge of North Collins.

Lying west of the stretch of Whittlesey shore described above
is an outlier of rock 3 miles long and half as wide which formed an
island in the lake. At the south end is a strong bar and spit on
which stands the Indian Council House and village, 14 miles west
of Lawtons. Strong cliffs or bars lie along the west side of the
island, where the full force of the Whittlesey waves was felt. All
about the north end of the island, which is 2 miles west of North
Collins, the shore features are strong and conspicuous, forming
a ridge under the road on the west side, and bars and cliffs just
above the highways on the north and east sides.

56 7 NEW YORK STATE MUSEUM

The Warren shores extend up the Cattaraugus embayment as”
far as Versailles, as already stated. On the north side of the creek —
the shore has not been traced, but it appears west of Fenton and
south of Brant in four broad sand bars running northeast and ~
southwest across the highways at Brant. These are nearly of the
same hight, the westerly one on the curving margin of the
sand plain seeming the stronger, lying along the 760 contour of —
the map. These bars are lower Warren, and lie on the western —
edge of a great detrital plain which seems to have buried the

morainal surface, since the lower ground contiguous on the west —

is a pronounced moraine [see p 13].

The beach crosses the east and west road at the creek, east of
Brant, and extends northeast 3 miles to Pontiac. The higher War-
ren lies 12 miles east of Brant, on the east side of four-corners, and
follows along the north and south road for a mile, then curves around
to the east as a cliff in dark shale at the north end of the Whittlesey
island described above. Farther to the southeast the lower Warren
forms a bar at the four-corners 1 mile west of Collins, and near the
Whittlesey shore. On the road leading north from this bar at the
road corners are several bars at lower levels, the lowest along the
south side of the east and west Townline road, and about 15 feet
lower than the higher Warren.

The village of North Collins stands on a gravel plain some 20 or
25 feet under the Whittlesey level, which plain is probably a filling
dropped in the lake by glacial drainage from the northeast past
Eden; andthe complex of bars westward as far as Brant is the
work .of waves on the extended and sloping delta plain. The
altitudes at North Collins are generalized as follows: Whittlesey
850, higher Warren 800, lower Warren 780, using the railroad at
the village as 830 feet. The locality is one of special interest as
it has an unusual development of glacial lake features, which will
repay careful study and precise measuring.

North Collins to Hamburg. From North Collins to a mile beyond
Eden, a distance of 6 miles, the Whittlesey shore lies along the east
side of the highway and railroad mainly as a cliff, although the
cliffs may have been partly formed by glacial stream cutting.
Beyond North Collins for 2 miles it exists as a bar, and shows well
where it crosses the east and west road, 2 miles from the village.

Beyond Eden village the Whittlesey beach swings northeast,
and east of the south branch of Eighteenmile creek it forms a bar
along the crooked road 14 miles southeast of Eden Valley, and as
a cliff it curves around the high ground and crosses the roads lead-

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GLACIAL WATERS IN THE LAKE ERIE BASIN 7)

ing southeast and east. Northeast of Eden Valley 14 miles the
shore line lies around an island hill, with a spit on the southeast.
On the east side of the middle branch of Eighteenmile creek the
shore is a conspicuous cliff, curving in a half circle, convex to
north, about the high ground on which lies the junction of three
towns, and it ends as a bar spit northeast of four-corners, near the
' main creek.

The higher Warren carries the main highway all the way from
North Collins to Hamburg, about 1o miles. A mile north of North
Collins a good bar appears on the east side of the road, but from
there to Eden, a stretch of 4 miles, the beach is chiefly a cliff in shale
with a smooth slope on the west and no lower Warren level is repre-
sented. From Eden to Hamburg, through Eden Valley, the beach
consists of heavy ridges or bars except where cut by streams.

The lower Warren features are represented on the plain west of
Eden and Eden Valley by a complex of bars and sand knolls,
some of the stronger bars being followed by the highways. The
area is sandy and seems to have been spread with the finer detritus
carried into Lake Whittlesey by the glacial drainage from the
northeast. The bars and spits which have been noted from the
roads are indicated on the map, plate 4. The road winding
westward from Eden follows a series of overlapping bars which
together form a broad low ridge. Taking the railroad at Eden at
788 feet the upper Warren level in the village is 802 feet. At Eden
Valley a good bar close to the railroad station is 5 feet higher than
the latter, or 783 feet, and is the lower Warren, while the upper
Warren at the village east of the creek is about 800 feet. The bars
and spits on the plain are at various low levels and decline westward.
They were probably formed by the agitation of the waters offshore,
and partly during the subsidence of the Warren waters at the
extinction of the lake.

Hamburg stands on the western edge of a delta built in Whittlesey
waters by glacial drainage from the northeast and later in Lake
Warren by Eighteenmile creek. Running northeast and southwest
across the plain is a frontal bar which supports the main. streets.
In the southwest part of the village the bar has an altitude of 807
feet, using the railroad as 789 feet. This is a precise elevation for
‘the upper Warren.

Hamburg to Spring Brook (Cazenovia valley). In this section
the Whittlesey shore line is discontinuous and the fragments are
not wholly located. Up the valley of EHighteenmile creek the shore
is a cliff north of North Boston along the east side of the highway.

58 NEW YORK STATE MUSEUM

Chiefly as a cliff it follows for about 3 miles along the roads leading
north and then northeast. Newton cemetery is located on a
gravel bar by a small creek. At the second three-corners the beach
is a good bar with a stream-cut bank on the southeast.

At the four-corners, 1 mile southof Dewell’s five-corners or 2 miles
south of Orchard Park, the steep bluff shown in plate 12 was
probably washed by Whittlesey waves, though primarily formed
by river work. North of this bluff and south of the five-corners is a
hill which was an island in the Whittlesey lake. :

Leverett makes the Whittlesey beach cross the moraine at
Orchard Park and follow along its north face [see ms pl. XXV].
This is a mistake, for the Hamburg moraine was laved by Warren
waters along its entire north face from Hamburg to Aiden, and the
moraine covers all the area between the Whittlesey and Warren
shores. The Whittlesey beach is an irregular line winding through
the moraine from 1 to 2 miles south of the Warren shore.

Orchard Park is below the Whittlesey, which is represented by
bars at 880 feet, crowning the cemetery ridge east of the village and
another ridge farther northeast.

Between here and Cazenovia creek no good features are noted,
but the shore lies around the north face of a large hill west of the
creek with the two ends of the half circle lying across the east and
west ‘‘Mile Strip’’ road. On the east side of the creek the Whit-
tlesey bars are more continuous, as will be noted in the next section.

Hamburg stands on the upper Warren bars with altitude of 807
feet. The lower Warren is conspicuous, forming heavy bars
carrying ridge roads west and north of the village, and with alti-
tudes 792, 789 feet and declining. The strong upper Warren bars
are followed by the highway leading northeast to Abbotts Corners
(Armor). At the four-corners south of the fair-grounds and 14
miles northeast of the village the beach is a series of parallel bars
which unite toward Armor.

The most extended and continuous ridge of the lower Warren
series between Brant and Spring Brook is the bar called ‘Coopers
ridge’’ which supports the road leading west from Hamburg to
Lake Erie. The bar extends west about 4 miles, nearly to Wier’s
brick works, south of Wanakah station. The head of the ridge is
about 790 feet, or 17 feet under the upper Warren, but the bar
gradually declines westward until it is lost in the silt plain at about
750 feet altitude. Like the lower bars at Eden and Eden Valley
this long bar projects away from the Warren shore out into the lake,
with falling altitude.

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GLACIAL WATERS IN THE LAKE ERIE. BASIN 59

Branching from the Cooper ridge near its head is a slightly
higher bar, 793 feet, swinging northeast across the railroad to the
north-leading road, and then lying parallel with the latter road.
One half mile farther northwest, at three-corners, another good

_bar occurs across the road and carrying the ridge road which leads

northwest, crossing the railroad and electric line. After supporting
the road for a mile the bar swings away to the southeast and passes
across the Erie county fair grounds. The east entrance to the

enclosure of the fair grounds is on this lower Warren bar, which

curving around to the northeast lies on the north-facing slope
of the strong upper Warren and about 20 feet lower. This lower
Warren is a well defined bar on the road leading northwest from
Armor, only about ro feet under the upper Warren at the corners.
On the north road the lower Warren supports the village cemetery
and then passes to the east side of the road and lies along the flank
of the upper Warren, with a vertical interval of to to 15 feet. For
24 miles from here, to north of Orchard Park, the upper Warren is
mainly an irregular wave-cut cliff in the north border of the moraine,
while the lower Warren consists of broken ridges and spits. North
of Orchard Park, toward Websters Corners, the highway lies
between the Warren bars, the upper and double ridge on the east
side being about 15 feet higher.

At Websters four-corners the lower Warren forms a great recurved
hook, convex northwest, which crosses the east and west road 4
mile west of the corners, and curving back towards the corners
makes nearly a circle. Another bar lies farther west across the
road, and another east of the corners on the north side of the road.

From Websters Corners to Spring Brook the Warren shore is
irregular but fairly shown on the map with reference to the roads
as broken and eroded bars and cliffs, along the face of the moraine.
The Whittlesey lies landward in the moraine. The definite north
edge of the moraine is an effect of the wave erosion. :

Spring Brook to West Alden. In this section the Whittlesey
shore line terminates.

On the east side of Cazenovia creek and south of Spring Brook the
Whittlesey shore lies along the angling roads as distinct cliffs or bars,
as Shown in the map. They follow the 900 foot contour, lying at
about 905 feet. A good display is found at the three-corners, 1
mile southeast of Spring Brook, where all three roads lie on the

bars with a spit lobe forming the knoll on the northwest road.

South of Elma Center station, 2? mile, the shore lies around the
north point of a hill, crossing the road under the houses of Henry

60 f NEW YORK STATE MUSEUM

Klem and Mrs John Krohn. It is here 70 to 75 feet over the lower
Warren at Elma Center station. Beyond an embayment on the ©

east, reaching up the hollow followed by the Pennsylvania Rail-
road, it again forms a curve about the north side of another hill,

and crosses the road north of three-corners, on the brow of the hill

under the house of Mrs Clark. The beach altitude here is 905 feet,
or 70 feet over the lower Warren bars at Steitz corners, 1 mile north.
These latest formed fragments of the Whittlesey beach are incon-
spicuous bars and would not be seen without search, but they can
be readily found by their relationship in altitude to the Warren.

It is an important and interesting fact that the vertical interval
of about 70 feet between the lower Warren and the Whittlesey re-
mains the same throughout the whole extent of the Whittlesey
shore in New York. ;

These are the most easterly features which can with confidence
be attributed to Whittlesey waters. A good example of a glacial
outwash gravel plain 1 mile east of Marilla, at 915 feet is perhaps
not too high for the Whittlesey plane. We here take our leave
of the expiring Lake Whittlesey.

In this section the Warren shore features become strong and
continuous. The village of Spring Brook lies on the Warren
beach. About 1 mile east of Spring Brook the higher Warren holds
the Tillou cemetery on the south side of the road, while on the
north side the conspicuous inferior Warren is 12 feet lower. East-
ward where the road crosses a creek the lower Warren is a strong
bar 4o rods north of the road, while east of the gully the road is
on the higher Warren. The two strong bars continue northeast-
ward in excellent form to Elma Center Station, where they divide
to make a close set series of gravel ridges, crosscut by the railroad.
The station lies in the cut in the line of the lowest (north) bar,
which is 835 feet altitude, taking the railroad as 824 feet. The
highest bar of the series is only 8 to 10 feet higher, but a cliff shows
higher wave-work.

Northeast, past the Lutheran church and cemetery, to Steitz
corners (or Bullis corners), a distance of nearly 2 miles, the Warren
beach is an excellent display of broad bars of fine gravel. At the
church the beach includes four bars in a width of + mile, and is
essentially a gravel plain with rolling surface. At Steitz
corners the series of several bars lie on the delta built in lake
Warren by Buffalo creek. West of the corners the delta plain has
an abrupt front 20 feet high, facing the low swampy lake bottom
plain. The altitude of the lower Warren at Steitz corners is 835

feet:

.

GLACIAL WATERS IN THE LAKE ERIE BASIN 61

South from Steitz Corners five higher bars appear, crossing the

road, the highest lying about 4 mile south and 17 feet above the

bar at the station, or 852 feet.

One half mile east of Steitz Corners, on the combined delta of
Buffalo and Little Buffalo creeks, the upper Warren appears as a
good gravel ridge lying across the road just east of the four-corners,

on the west face of the moraine, with altitude of 846 feet. The
lower Warren occurs as two bars obliquely crossing the north-
_ leading road and with a pronounced hollow between them. East

of Little Buffalo creek the several bars occur in strength, crossing
the highways obliquely.

Northwest of Marilla on the north and south Townline road the
beach is represented by four strong bars distributed through over
a mile and vertically spaced through 20 to 2s feet. The Zion’s
church at the four-corners stands between the two middle bars.
The two bars north of the corners are about 2 feet higher than the
corners, or 832 feet. The highest bar is # mile south on the north
bluff of the Little Buffalo creek, near three-corners, and has an
altitude of about 855 feet.

On the road leading east from the four-corners at Zion’s church the
highest bar is contoured as 860 feet. The beach holds steadily
the northeast direction all the way to West Alden but with variation
in the number and strength of the bars. On the north and south |
road passing through Marilla three strong bars lie north of the four-
corners, the lowest being at the angle of the road under a school-
house, with a low swamp lakeward, and with altitude by the con-
tour of 840 feet. The middle bar is about 11 feet higher.

Continuing northeastward the bars cover another four-corners
south of Cayuga creek, the highest bar passing to north of the
east-leading road.

North of Cayuga creek, at West Alden and Alden, is an unusual
display of bar ridges. On the West Alden section seven strong
tidges are found, the lowest under three-corners at 830 feet, the
highest over a mile landward at over 860 feet. The West Alden
corners lie on the fourth ridge with altitude 845 feet.

West Alden to Fargo station; to Crittenden: At West Alden the
Warren bars divide into two sets, the southerly and higher bars
passing northeast through Alden and on toward Fargo station,
terminating between the station and the Countyline road, while the
lower series leads northward by Alden Center to Crittenden and
continues as the Warren shore through central New York.

Alden lies on a delta built by glacial drainage from the east and
four bars pass northeast through the village, the higher one being

62 NEW YORK STATE MUSEUM

860 feet. Two of these bars continue northeast nearly 3 miles and
end $ mile beyond the Countyline road, on the Fargo delta. These
are broad ridges composed of the shale detritus supplied by the
glacial drainage of the channels along the line of the Delaware, —
Lackawanna & Western Railroad. They are of nearly the same ~
hight, 865 and 863 feet according to the map altitudes. The
Countyline cemetery is located on the northern ridge.

The splitting of the Warren shore into two series of bars might
suggest a dual lake history, or at least two stages of the Warren
waters. The phenomena have the same origin and significance as
the multiplicity and large vertical range of the bars on all the shore
to the westward, considered along with the greater simplicity of
the shore features from here eastward. The complex problem
of the lake records and history will be considered later [see p. 64].

The difference in altitude between the Alden-Fargo and the
Crittenden bars is very slight, though the northward uplift of the
land surface should have some credit for the present equality in
altitude. The Countyline cemetery bar is 863 feet, the Crittenden
bars are 857-860 feet. In the 11.5 miles from Elma Center station
to Crittenden the uplift is not over 25 feet, or a trifle over 2 feet a
mile in the direction of the shore. Between the cemetery and
Crittenden the uplift can not be over 6 feet, which makes an original
difference of about 1o feet. It would seem that the element of
altitude was not a strong factor in the case. The writer regards
the separation of the beaches as largely an accident of the topog-
raphy, along with some falling of lake level while the ice front was
in this locality.

Another noteworthy feature connected with the strong bars all
the way from Steitz corners to the end of the Alden series, about
9 miles, is the occurrence of pronounced swamp hollows lying be-
tween the bars. These sometimes resemble drainage channels and
in a few cases are now occupied by brooks. Emphatic hollows
between beach ridges are not uncommonly seen forshort distances,
but the writer has nowhere else found them so strong and per-
sistent. The location of the hollows as between lower or higher
bars is indifferent.

The northern series of bars swing northerly at West Alden and lie
on the east side of the highway at Alden Center, where they are
broad flat ridges of shale detritus on the banks of Ellicott creek.
The bending road follows the bars to the West Alden station of the
Lackawanna Railroad. At this point a moraine ridge stands
inclosed in the shore deposits. North of the railroad and the
moraine area four parallel bars lie oblique to the north and south

GLACIAL WATERS IN THE LAKE ERIE BASIN 63

road. The lowest, with altitude 847 feet, lies under the highway
_ north of the overhead crossing of the Lehigh Valley Railroad and
_ its north end swings around east as a recurved hook. The higher
_ bar lies 4 mile east, and is occupied north of the Lehigh Railroad
_ by the Crittenden highway. Its altitude at the Lehigh crossing
is 857 feet. From this point north for about 2 miles the beach is
a single heavy bar, supporting the village of Crittenden. North
of the village the map gives the beach altitude as 860 feet.

A mile northeast of Crittenden the beach splits into a diverging
or fan-shaped series of bars with nearly equal altitude, lying on
the delta built in Lake Warren by the latest glacial drainage from
the east, along the track of the present Murder creek. The south-
ernmost bar lies along the north side of an east and west road;
the most northern bar pursues a northeast course and supports a
road for a mile, approaching Pembroke. The lakeward side of the
shore in this stretch of 8 miles is a steep slope facing low,
swampy ground.

The village of Pembroke lies on a shore or delta deposit of Murder
creek. Northeast from Pembroke for 14 miles the shore features
are too weak to map, but a good bar occurs a mile northeast of
Pembroke station under a north and south road, with its south end
curving east. Northeast of this bar and at four-corners south of
Indian Falls a bar is found supporting a cemetery, with elevation
of 869 feet.

Up to Pembroke the Warren shore has been found in the form of
heavy bars, with direct course, and for long stretches has developed
to maturity. From Pembroke and Indian Falls eastward through
central New York the bars are usually faint and the shore line is
weak and very immature. The Warren shore west of Crittenden
must have felt the wave work several times longer than the shore-
line to the east of Indian Falls. The conclusion is that the glacier
front rested for a long time on the high ground north and west of
Batavia, and the Warren waters were then dammed off from
the land to the east. Other glacial waters were, however, doing
their work in that region. When the ice finally gave way and
permitted the Warren waters to enter central New York, it was but
a relatively short time before they were drained down by eastward
escape and the Lake Warren extinguished.

From Indian Falls east to near Leroy the Warren shore lies along
the brow of the scarp of Onondaga limestone which forms
the high ground from northwest to northeast of Batavia.
The scarp was probably the result of long eras of preglacial

64 NEW YORK STATE MUSEUM

weathering with some modification by the ice rubbing. Through
considerable stretches the Warren beach lies on the top of the
ledges and is marked by the deposits of angular chert gravel, which
the farmers call ‘‘chawed rock.’”’ Such is the case from Indian
Falls eastward for 4 miles. In some stretches the shore is a lime-
stone cliff, some striking examples of which are seen south of South ©
Alabama (east and west of “‘Pond’’ survey station, northeast and
east of Batavia, and west of Morganville).

In 1896 the Warren shore was traced in a general way, chiefly to
prove its continuity and altitudes, from Crittenden around into the
Genesee valley. The topographic maps were then not available
and the plotting was done with reference to the roads. The bars
are so weak and discontinuous that mapping is difficult and unsatis-
factory even with the help of the topographic sheets.

As the province of this treatise is only the portion of the Erie basin
lying in New York we will leave the Warren shore at its extreme
north point, the limestone ledge at Pond station, 1 mile south of
South Alabama, where its altitude is 887 feet.

Discussion of Whittlesey and Warren levels

The duality or multiplicity of the bars on the Warren shore,
giving occasion for different names and the conception of two
distinct lake levels, has been stated on page 45. Having now
before the reader the detailed description of the shore features we are
better prepared to discuss the causes and significance of their
complexity and of the lake history.

The difference in complexity between the Whittlesey and
Warren beaches is very marked. In all the Erie basin the Whit-
tlesey beach is commonly a single ridge, which doubtless represents
the wave-work at the surface and margin of the lake, while on the
same slope the Warren shore, about 4s feet lower, has several
ridges ranging through to to 30 feet vertically. However, the
Warren shore is commonly more simple from Crittenden eastward,
and the interesting problem discussed in this chapter is the cause of
Warren complexity west of Crittenden as compared with the relative
simplicity eastward.

The following table shows the vertical spacing of the bars, both
Whittlesey and Warren, at many points along the shore. The
figures are not precise, some being by aneroid, but all are carefully —
checked. Doubtful figures have been omitted from the table, and
the errors are not greater than is the local variation in the individual |
bars. The tendency to read the aneroid in multiples of 5 feet 1s

GLACIAL WATERS IN

THE LAKE ERIE BASIN

x

_ shown in the table, and the errors are certainly within that amount.
A few accurate beach altitudes are included in the table.

TABLE OF VERTICAL SPACING BETWEEN WHITTLESEY AND WARREN BARS

LOCALITY

Sas. Lita Iago ae ee
CREW OURADICY.. o..6..- «
JRGVONGN6-3.0 bce Se ees oleae
1m.e. of Ripley
Mee OmMOLsyil. w.. so. ass
ite eeOnMorsybh...2.. .
Im.s.w. of Westfield
WMiestiiel eels a cose ale
4m. w. of West Portland..
West Portland (brick

Ce eC i ey

eooae

CC ee
eo eee
Ce

24m.n.e. of Fredonia.....
Sheridan

Ce CC
ee ee woe
eoees

14 m.n.e. of Hanover Cen-
betes ;

Gy aale e “by n. from Han-

over Center...........

34 m. e. of Hanover Center

INorthyCollinss sce. 5. o.

rm. w. of North Collins...

2m. w. of North Collins..

ce eee eee e fe © © wee oe 8 oo

eee se ee eo eo eo oo

1S ait Siok eee ete eee
2m.n.e. of Hamburg (fair
grounds)
Armor

ee 2 © © © © © wo ow
Se

eee eo oe ow

Tillou Cemetery (1 m. n.e. of

PHU BrOOk) oi. cee hee.
Elma Center station
MIPEIEZEC OMICS ona we soe! vite:
Zion’s church (2 m. n.w. of

AVA ea ret eas) cae ees Fo 28 Sela ai ee
West Alden
JANCIS Speen Mise SERGE ge SI
Countyline onery (2 m.

n.e. of Alden)
Crittenden

eceee ee ec ec oe eo ew

ese oe oo eo ow
eere2ee ec eo ee oe oe

eee eee ec ee oe oe

Pond station (s. of South
Alabama)

eceee ee ee se eo oo

Interval
in feet
between
Whittlesey
barand the
highest
strong
Warren bar

ee eee eee

eee ce © © © eo
eee eee ee

eee eae eo

ee ee soe oe

ee oe ee oo
ee oe eo eo

Upper
Warren
altitudes

see coe ew
eee ec eee
eee ee eo
ee ee ee ow
ee eee eee
cee eee ee

eo cece eee
cece ee ee

eo ee ee ee
ee cee eo

eee eee ee

eee eee ew
eee eee ee

eee ee ee

ees ee eee
eee ce eee

ee ee ee eo

eee ee ee ele

ee oe ee eo

eco eee eo

ee ec ee oo

eco eee oo

ee oe eo ©

ee oe eee e

eee ce eee

Interval
in feet
between
Hieber and
lower War-
ren bars

ee ee 8 oo eo

ee oe eo oo

ee ee ee ee

eee ceo eo

Lower
Warren
altitudes

ee oe ee oe
ee oe ceo ee
ee 2 ee ooo
eee ee oe o
Ce Ce
eee eee oe
ee eee eo
ee cee eo oe

ec eee eee
eee eee eo
eee ee eo
ee ee eee
eee ee eee
eee eee ee
ee cece eee
ae ee ee oe
oes eee ee
eee cee oo

eo 20 eo 6 © oo

ee eee eo
2 8 0 © © oo o
eo 2 ee oo 0
ee ee eee oe
ec eee oo

220 ee eo ©

Ce ee

ee e202 © ©

eeeee ee eo

e200 e 8 oo

eee ee oe eo

eo 0 e8@e0e 20 ©

eos eos oo

66 "NEW YORK STATE MUSEUM

The above table shows that the vertical interval between the —
Whittlesey beach and the highest Warren is commonly about 45 to
so feet. The interval between the highest and the lowest Warren
is relatively more variable, but the two intervals added together
generally make a total range of about 70 feet between the Whit-
tlesey and the lowest good Warren bar.

The vertical range of the Warren bars is thought to be greater
than is usually possible for strong offshore or submerged bars in a
body of fresh water having a steady surface or only a single level.
That the higher and stronger bars represent a lake level of long
endurance can not be doubted. They represent a water level,
and the problem before us relates to a second or lower lake surface
in explanation of the lower bars. The following suggestions are
proposed.

t The lower and multiple bars might be the effect of very slowly
falling waters, with or without long pauses, produced by the down
cutting of the lake outlet.

2 The vertical spacing might be due to progressive differential
uplift or tilting of the land during the life of the lake.

3 The lower bars long ago suggested a second distinct lake level,
and the names “Arkona’”’ and “‘Forest’’ have been used by some
authors for the upper and lower bars which in this writing are
collectively called Warren.

4 The lower bars may, at least in part, represent the offshore,
submerged sand ridges formed by the drag of heavy waves along
with the transporting effect of shore currents.

In discussing the above explanations of the multiple bars the
following facts should be considered:

a The practical absence of inferior or secondary bars of much
strength along the Whittlesey shore. From the Whittlesey ridge
down through the 40 to 50 feet to the upper Warren level, bar ridges
are commonly wanting.

b The multiple Warren bars occur in strongest development on
delta tracts or where abundant detrital material was available for
ridge construction: for example, at State Line, Portland, Hanover
Center, Brant, Eden, Hamburg, Elma and West Alden.

c Eastward from Crittenden or well beyond the Whittlesey area
the Warren shore becomes simple and resembles the Whittlesey.

d In New York the Whittlesey was inaugurated as a primitive,
invading lake, on the land surface abandoned by the ice sheet.
The Warren water, on the other hand, was not inaugurated wholly

GLACIAL WATERS IN THE LAKE ERIE BASIN 67

by the invasion of a new body of water, but as far east as Marilla

it was produced by the lowering of Lake Whittlesey or other waters.

eé The complex Warren shore lies on a plain of slight incline and

low relief which was the silted and filled lake bottom of the preceding
_ Whittlesey, while the earlier and simple Whittlesey lies on the higher

and steeper slope. From State Line to Silver Creek the land slope
is uniform with no very heavy deltas or detrital fillings, and the
Warren bars are close set and parallel. On the plains between Silver

Creek and Hamburg, flat and silted, the bars are scattered. From
Hamburg to Alden the bars are multiple but strong and compact.

The divergence of the bars at West Alden into two sets seems to

be an accident of the topography and the tributary ice border
drainage. From Crittenden eastward the shore has more sim-
plicity, as stated above. |

j Multiple bars are regarded as the characteristic product of
long-continued work of waves and shore currents in waters of
comparatively steady or slowly falling level, and are consequently
found in greater. development along older and. maturer shores.
It is uncertain to what extent submerged bars can form in water
which has very changeable or rising level, but such conditions are
believed to be unfavorable.

g The depth of effective wave action in fresh waters has not been
determined precisely, but it has been regarded as not over 30 feet.
Supposing the Warren bars to represent a single level, the table
of vertical spacing would indicate that the depth of bar construction
could not commonly exceed 25 feet.

h A young outlet of insufficient capacity might involve consider-
able fluctuation of lake level by the damming of high waters. This
would apply much more to Whittlesey than to Warren, because the
Warren outlet had been previously the ultimate outlet (from Lake
Saginaw) during all the life of Whittlesey.

_. With the above facts and principles before us we will now discuss
the suggested explanations for the lower Warren bars.

1 The multiple Warren bars could not have been the product of
lowering waters during the extinguishment of the lake or they
would not be so uniformly limited to the belt covered by 70 feet
under the Whittlesey plane, since the waters fell through the entire
vertical distance to the present Erie. The bar phenomena which
actually were produced by the subsiding or hypo-Warren waters
are described below and we find that they are scattering and rela-
tively few. Even those of the Dana level are disappointing,
though generally recognizable.

68 NEW YORK STATE MUSEUM

A peculiarity of the strongest bars which belong to the phase of

the falling waters is their direction transverse to the shore. Exam

ples are Cooper ridge at Hamburg, the ridges at Eden and North ©
Evans, as well as the Dana ridge at Evans. Instead of being
parallel to the shore like normal shore bars they are directed into
the lake, and decline in hight. The mechanics of the constructional —
operation is not clear, but the peculiar result in the bar form is —

evident.
It is again pertinent to repeat that the whines shore has

practically no inferior bars, yet the lake was a large water body ~
with twice the area of the present Erie, and the broad surface could |

not have lowered suddenly.

The objections to formation of bars at lower levels by falling
waters does not apply with force to extremely slow subsidence, and
it seems likely that such a series as the Warren bars, strong and

irregularly spaced, might well be produced by the very slow falling ~

of the surface due to the down cutting of the lake outlet, or to the
extremely slow tilting of the land due to unequal uplift. This will be
discussed later.

2 The splitting of the bars, with increasing vertical spacing, due
to differential uplift or tilting of the land during the life of the lake
is theoretically probable. The New York area lies north of the
isobase or line of equal tilting drawn through the Warren outlet in
Michigan, and any northward uplift or canting of the land during
the existence of the lake should produce a separation of the beaches.
With such origin the series of bars should manifest some divergence
among themselves, or a range of vertical spacing increasing north-
ward. Such is not readily apparent, for the vertical relation of
the Whittlesey and Warren bars remains nearly the same through
the 75 miles of shore line, though in that distance the whole double
shore rises 122 feet. However, there are complexities in the study
of shore deformation and bar divergence, and a small amount of
divergence in spacing would be difficult to measure.

The diagram [fig. 4] is intended to indicate some of the difficulties
in the study of deformation of shores formed in front of receding
ice margins. Leverett has shown that west of New York the
deformation of the shores is very slight. In New York there is an
increasing deformation [see p. 77] as we pass northeastward, so
that the uplift toward the termination of the Whittlesey beach at
Marilla is 2 feet a mile. Taylor has concluded from a study of the.
features in the critical district of the Whittlesey outlet that the
Whittlesey beach was produced in slowly rising waters. If this is the
fact it would neutralize the effects of slight land warping.

;
‘
7

GLACIAL WATERS IN THE LAKE ERIE BASIN

West of the Marilla-Alden district the Warren
bars were not formed at the ice front but were
produced synchronously throughout the entire
extent by the falling from the Whittlesey level.
These bars should be continuous and should re-
cord among themselves all the divergence due to
land tilting, but this effect is so small in the area
of New York that it must be obscured by the
constructional irregularity of the bars.

East of the Marilla district the Warren waters
laved the ice front and from there eastward the
bars should have the fragmentai character due
to a shore line extending toward receding ice

while the land was tilting. But here the life of.

the lake was briefer and eastward the bars are
not sufficiently developed to yield any reliable
data.

The diagram shows that the bars formed in
front of the receding ice margin are theoretically
not continuous or in the same plane, but that
they represent successively lower planes. Con-
sequently our measure of deformation on such
shores fails to show the full amount.

The above may give some idea of the
quantitative difficulty inthe study. The series
of Whittlesey-Warren bars seem to retain a
practically uniform relation and it seems quite
certain that most of the land tilting which has
occurred took place subsequent to Warren time.
Nevertheless it seems probable that a small
amount of deformation which may have taken
place during Warren time helped to produce the
multiplicity of bars and the large vertical
spacing in New York.

3 The conception of a second water level was
the very natural explanation of the considerable

vertical range of the Warren bars, specially as

in some localities only two conspicuous ridges
are found. Objections to this explanation are
the decided lack of uniformity in relative
position of the lower bars, and the equally de-

Whittlesey beach

=

shore

Vfarrei

—\

Fig. 4 Diagram to illustrate theoretic tilting of shore lines

790 NEW YORK STATE MUSEUM

cided lack of horizontal uniformity and continuity. A lowes j

water level should have been steadier than the superior or original
level for the reason that the outlet was more mature and the lake

7
;
.

larger in area. The lower Warren bars are sufficiently strong to

have great continuity and uniformity of level if their formative

conditions had favored it, but no separate or distinct water es
can be selected among the lower Warren bars.

4 The idea that the inferior Warren bars are chiefly the Be a
product of offshore waterwork in a lake of long life with very slowly
falling surface would seem to harmonize the facts of variable
altitude, horizontal discontinuity, generally finer material, and
as a rule more rounded or flatter summits.

The incomplete data gathered in the table [p.65] indicate that
a depth of 25 feet below the upper bar is the limit of effective bar
construction. This figure may be reduced by whatever lowering
of the surface level is to be allowed, and 5 feet may be taken out for
the hight above the water surface of storm bars of coarse material.

‘The mechanics of the deeper work of the water is not well under-
stood, but theoretically it would appear that the first offshore bar
must lie below (in depth) and beyond (in horizontal distance) the

zone of action occupied by the heavy waves which build the surface:

or marginal bar. The vertical distance between the marginal and
the nearest submerged bar is greater (within limits) as the hori-
zontal distance is less. It would appear, therefore, that normally a

striking vertical interval might lie between a heavy marginal ridge.
and the first submerged bar, sometimes suggesting two distinct:

water planes.

It is apparent that the bar elements will vary with several factors:.
the topography and slope of the bottom, the volume and character.
of the detritus, the exposure to winds and depth of water, and the -

effectiveness of shore currents. It is not now possible to apply

these principles to the case in hand. The factors in waterwork:

are so delicately adjusted and (to our sight) so capricious in their

-operation that they are elusive to study. It is very desirable that .-
an examination of existing lakes and seas should be made with ~

reference to the offshore constructive features. And we specially
need criteria for distinguishing phenomena -produced in slowly
rising water from those produced in slowly falling water.

The absence of inferior bars along the Whittlesey shore may be.

due to the steeper slope, the more variable and perhaps rising

water level, and the brevity of the life of the lake. The last factor

is the probable explanation of the simplicity of the Warren shore
east of Crittenden.

GLACIAL WATERS IN THE LAKE ERIE BASIN 71

The multiple Warren bars probably represent only a single lake
or a lacustrine unit with some change of level due to land warping
and lowering of outlet, the lower bars having been formed as off-
shore ridges, in waters of long life, supplied with abundant detritus.
_ Since the above was written Mr Frank B. Taylor has announced
the discovery of a complication in the glacial lake history, of which
a brief statement has been inserted on page 42. Quoting his
words from a letter: ‘The ice front on the “‘Thumb”’ of Michigan
retreated in an oscillating manner with marked readvances covering
a space of 20 to 25 miles in each readvance, and the Belmore (Whit-
tlesey) and Upper Forest (Warren) beaches each records such a
readvance, which raised the lake level.”

Taylor’s theory is that with the draining down of Lake Maumee
the waters continued to fall to the Arkona level where they rested
a long time, until a readvance of the ice front again closed the Arkona
outlet and forced the lake waters up to the Whittlesey level. In
other words, a lake (Arkona) approaching the Warren level existed
in time between the Maumee and the Whittlesey, but lower than
either. 3

The vertical intervals between these several lake beaches in
Michigan are given by Taylor as follows: Between Whittlesey and
upper Arkona, 30 to 31 feet; between upper and middle Arkona,
7 to 8 feet; between middle and lower Arkona, 8 feet, or a range
of Arkona bars of 15 to 16 feet; between lower Arkona and Upper
‘Forest, 14 to 17 feet. (It should be noted here that no such vertical

relation occurs between any beaches in New York.)
_ The theory has been held by Taylor that the ice front in the
Erie basin oscillated synchronously with that in Michigan, and
that the retreat of the ice front was sufficient to allow Arkona
waters to extend into central New York. In order to test this
theory by the facts the following analysis is given.

Assuming Taylor’s interpretation of the glacio-lacustrine history

to involve the Erie basin, then one of the three following postulates
or some combination of them must apply to the district between
Cleveland and Crittenden.
A The ice front stationary. Under this conception the waters
of the three lakes, Maumee, Arkona and Whittlesey, would have the
same limitation and the beaches would all terminate together at
the moraine, and be wanting eastward. The channels of ice border
drainage and their deltas would end at the Maumee level.

B_ The ice front oscillating synchronously with the oscillations
on the “Thumb” of Michigan. The Arkona shore would form as
far beyond (eastward of ) the Maumee limit as the ice front receded

72 NEW YORE STATE MUSEUM

in Arkona time. Then the readvance of the ice (oblique to the
valley slope) would override and destroy a stretch of the Arkona
beach. (If the ice reached the Maumee limit the features would
simulate those in “‘A’’. The full-hight Whittlesey would extend
eastward only up to the advanced moraine, or only as far as the
undestroyed Arkona. In other words the Arkona and the Whittle-
sey would have the same eastward limitation. Both the Arkona
and the Whittlesey would terminate against a moraine with full
force instead of fading out. (Any recession of the ice during the
Whittlesey episode would cause some fading of the shore line.)

The ice border drainage in the eastward stretch from the ter-
mination of the Maumee shore to the Whittlesey moraine would
reach down to the Arkona level, except right at the moraine,
where it would reach only to the Whittlesey level. Beyond the
moraine, eastward, the glacial drainage would reach down to
the Warren level. (There would be no glacial drainage, only land
stream drainage, into the Whittlesey waters, except at the read-
vanced moraine.) .

C The ice front continuously receding. The Maumee bars
would fade out. The Arkona bars would extend farther eastward
and also fade out, but would be modified by the subsequent sub-
mergence. The Whittlesey shore line would reach still farther
east and fade out.

The ice border drainage in the Maumee territory would reach
down only to the Maumee level. Eastward of the Maumee limit
the glacial drainage would reach down to the Arkona level as far
east as the Arkona shore extended. Farther eastward this drain-
age would reach down only to the Whittlesey level, as far as that
shore extends, beyond which the drainage would reach down to
the Warren level. This is expressed in the following diagram,
in which heavy lines suggest the limits of glacial drainage.

1 Maumee

3 Whittlesey

Southwest
Northeast

4 Warren |

The following important facts bearing on the three postulates
may be restated.

t Obliquity of ice front. The New York edge of the Erian ice
‘lobe was oblique to the land slope, in consequence of which the

GLACIAL WATERS IN THE LAKE ERIE BASIN 73

advance or retreat of the ice front involved oblique overriding or

- uncovering of the slope.

' 2 Shore lines. The Maumee shore line does not reach into New

York, and is said to terminate near Girard, Pa. The Whittlesey

_ beach is a definite and generally simple ridge extending east to near
Marilla, or 100 miles farther than the Maumee. The Warren shore
comprises a series of multiple ridges or bars as far east as Indian

Falls, or r5 miles beyond the Whittlesey. From Indian Falls east
it is weaker, broken and simple.

3. Possible Arkona. The only bars which can be regarded as
Arkona are the higher ones of the Warren series. But these are
not subdued by drowning; they are stronger than the Whittlesey ;
‘they are less interrupted and generally stronger than the lower

bars; and they extend far beyond the limits of the Whittlesey.

4 Spacing of the beaches. The vertical distance between the
Whittlesey and the highest Warren bars is commonly from 45 to so
feet. The only instance of less spacing is southwest of Westfield,
where five sections have given records of intervals 35-40 feet.
The vertical intervals between the several Warren bars have no
steadiness which would indicate distinct lake levels. The total
range of the Warren bars is usually 20-25 feet, the greatest
ranges being on deltas, and only two exceptional localities giving
more than 25 feet. Some of the best sections, apart from deltas,
give ranges of 11-15 feet, with interval between Whittlesey and
upper Warren of 55-60 feet. The total range of the entire shore
features is about 70-75 feet. The Belmore-Arkona interval in
Michigan of 30-31 feet does not exist in New York.

5 Ice border drainage. The glacial drainage followed along the
receding ice front, and clearly marks the successive positions of
the latter. Thestreams debouched at the Whittlesey level as far east
as the levelextends. But beyond the Whittlesey limit, as at Alden,
Crittenden, and Fargo, the ice border drainage clearly reached
down to the Warren level.

Applying these facts to the three postulates of ice recession
the conclusion is that (A) and (SB) are emphatically ruled out,
and that (C) applies to the New York area only subsequent to
Arkona time. It is not doubted that the recession of the ice front
may have been unsteady, even in New York, but the practically
continuous recession in New York is in best accord with the dis-
covered facts. The Arkona beach does not appear to be repre-
sented in New York. The channels and deltas of glacial drainage
are clear, definite, unmistakable evidence of the ice limits and of
the lake levels. As far east as Marilla the ice border drainage

74 NEW YORK STATE MUSEUM

terminated at the Whittlesey level; eastward from this district
the glacial drainage is down to the Warren level. It seems certain
that the Whittlesey waters lay against the ice front while the
latter receded from State Line to Marilla, a distance of 75 miles.
The lake phenomena correlating with the ice front oscillation on —
the ‘““‘Thumb”’ of Michigan should be found, if found at all, in the ~
30 miles of shore line between Girard, Pa. and State Line.

Theoretically it would seem improbable that a great stretch of —
glacier front, given great lobations by the land depressions, and ©
with different conditions of latitude, climate, snow supply, direction .
and rate of flow.and push or impulse should oscillate synchro- —
nously. There isevidence, which will be published in a later writing, —
that as between the Batavia and the Syracuse districts the motion
of the ice front was a seesawing.

It is recognized that glacial and glacial lake history will be
found increasingly complex as facts multiply and it is granted
that some oscillation of the ice front was likely, but in the New
York portion of the Erie basin the facts thus far favor the simpler
history as outlined above. The records of ice border drainage
and glacial lakes east of the Erie basin, the description of which
does not belong in this discussion, seem to prove that no Huron-
Erie waters earlier and higher than the lower Warren ever extended
east of Crittenden.

Work of the subsiding waters: Lake Dana beaches

The general relation of the waters has already been given [p. 43],
and some discussion of the phenomena. We will now briefly
describe the features in order from west to east.

The time required for the lowering of the water surface from the
Hamburg beach down to the Erie level, 235 feet, must be estimated
in centuries if not in thousands of years, and we might expect to.
find some continuous beaches at intermediate levels. Although
all the slopes are subdued and evidently subjected to water erosion
and silting up of low places yet the phenomena as a whole are not
striking. A few strong bars are found at different levels but no
continuous shoreline.

Northwest of Westfield on the edge of the Chautauqua creek
delta, at Barcelona, is a good bar on the cliff close to the Erie shore..
Its height above the lake is 35 feet, making its altitude 607 feet. -

At the north edge of the city of Dunkirk are a good bar on the
lake cliff and a series of sand deposits which have been excavated.
The bar is 22 feet over Erie, or 594 feet altitude. .

EDUC
_JOF
STA

UNIVERSITY OF THE STATE OF NEW YORK

EDUCATION DEPARTMENT
JOHN M CLARKE STATE MU UM BULLETIN 106 PLATE 22
STATE GEOLOGIST SE PART OF SILVER CREEK QUADRANGLE

2fGilometers

Contour interval 20 feet, / / / ;

Datum is mean sea level, | | |

LEGEND

H. L. Fairchild 1905

Se TM eels,

mn
nS Y

GLACIAL WATERS IN THE LAKE ERIE BASIN 75

Several bars occur in the vicinity of Silver Creek. The strongest
is over a mile southwest of the village on the 720 foot contour,
crossing a north and south road. Other shore featires lie east and
northeast of the village, the highest being on the slope of the hill
along the 700 foot contour. The lowest crosses the road leading
to Irving at about the 600 foot contour.

North of Farnham 14 miles a faint bar was seen on the east side
of Muddy creek at the angles in the road, coincident with the 600
foot contour.

Conspicuous and extensive sand bars occur at Evans village,
north of Angola, on the delta of Big Sister and Little Sister creeks
[pl. 22]. The road from Evanstothe lake along the north side of the
creek lies on these bars for nearly 2 miles. The south street of the
village is on a bar that passes west around the slope. In the village
the bars are on the 620 foot contour and lower, while the ridge
road is on the 600 foot contour. These beaches belong to the Dana
level, and other correlating shore features occur northward on the
600-620 foot contours for 4 miles. A strong bar lies north of the
road on the west side of Pike creek, near its mouth.

On the plain west of Eden and Eden Valley are extensive sand

-tracts and bars much below the Warren level. One leading west

from Eden carries a curving road for 2 miles and resembles the
Cooper ridge at Hamburg. Somewhat similar phenomena occur
at Eden Valley Station, and in both cases they have lower Warren
level at the eastern end but decline westward.

At North Evans there are strong bars on the delta of Eighteenmile
creek, which seem to be over 700 feet altitude. The heaviest bar
supports the road leading west from the corners, crossing the
railroads and then turning south. Another bar lies north of the
creek under the highway. :

The strong bar called Cooper ridge, leading west from Hamburg

for 4 miles, has been described on page 58. This declines from
790 feet altitude at Hamburg to toward 700 feet at the fading
western end. It could not have been wholly formed during the
life of Lake Warren at the full Warren level, but apparently repre-
sents continuous construction in the falling waters. The ridges at
Eden and Eden Valley have similar relationship and genesis.
_ The east and west ridge at West Seneca, south of Buffalo, sup-
posed by Leverett to be a beach [Monogr. XLI p. 772], is amorainal
ridge of till with only a thin and patchy veneer of sand. The other
ridges and knolls in the vicinity are also till, including the ridge at
Ebenezer which is a continuation of the West Seneca Moraine ridge.

Some of the shore features mentioned above were first noted by

76 NEW YORK STATE MUSEUM

Leverett, who speaks of seeing other evidences of lake work at
various levels from 30 to 60 feet over Erie. The writer also has
observed many such features that are too faint or uncertain to map.

The most interesting of the hypo-Warren phenomena are those
which belong to Lake Dana and which include several of the
bars noted above. This lake had a level about 180 feet under
Warren. Its shore features are usually weak in western New York,
but can be found in favoring situations at the proper level.

At Pine Hill cemetery, in the northeast part of Buffalo, and
northward near the city line, are well developed Dana bars, on or
over the 700 foot contour [pl. 23]. Northeastward in the town
of Alabama and specially in Elba there are spits on nearly all the
drumlins which rise above 700 feet. These are often indicated by
the numerous gravel pits, and are well displayed north of Elba
village.

Through central New York the shore line retains the altitude of
about 700 feet, and strong bars occur west of Geneva and at Fayette,
‘east of Seneca lake.

The shore phenomena of Lake Dana should be found throughout
the Erie basin at the following altitudes, which are determined by
subtracting 180 feet from the Warren altitudes in the corresponding
localities.

Altitudes of the Dana plane in the Erie basin

Northeast of Buffalo, at 680 to 690 feet altitude
Buffalo, 660 to 680 feet
South of Buffalo, 630 to 650 feet, or 60-80 feet over Erie
North Evans, 610 to 630 feet, or 40-60 feet over Erie
Evans, 600 to 620 feet, or 40-50 feet over Erie
Irving and Silver Creek, 590 to 610 feet, or 30-40 feet over Erie
Dunkirk 575 tougas feet, Or tp to 25 teetrover sine
Brocton, 575 to 585 feet, or up to 15 feet over Erie
Westfield, 575 feet and under, or at Erie level

By comparison with the above table it will be seen that the bars at
North Evans are above the Dana plane, as are all the bars on the
lake bottom plain between Hamburg and Brant. But the bars at
- Evans and north, the lower bars at Silver Creek, and the bars in
the north edge: of Dunkirk fall in the Dana plane. Many other
correlating features will be found by any one who looks for them.

Deformation of the shore lines; land warping ©
The shore lines of the ancient lakes must have been originally
horizontal, but they are not so now. In all the region of the
present Great Lakes the northward rise of the beaches is evident

za UNIVERSITY OF THE STATE OF NEW YORK

EDUCATION DEPARTMENT STATE MUSEUM
JOHN M. CLARKE i
_ STATE. GEOLOGIST

BULLETIN 106 PLATE 23
PART OF BUFFALO QUADRANGLE

7845°
43
lore}

Cheektowagal—.

ee: =
| ES ——

Aa ANIL
Pant!

: H. L. Fairchild 1905
LAKE DANA BARS NORTHEAST OF BUFFALO

palm et Detect) oe eee er ie he ‘aki i¢ Pitre
‘ le é ] Shik es arp ot Yow |

ete iolicsyes 3156 roe Pe,
hi CREA ESR: UO. TRA aie et PE Eh

i vats
3

t

7) th hotel Mtns, Te ROT tery Raita Ce 1 ORS erate

GLACIAL WATERS IN THE LAKE ERIE BASIN Tea

proof of the recent tilting of the land surface. In other sections
of the continent land warping may take place without any visible
7 indication of the movement, but in this area of the Great Lakes
the deserted shores of the “fossil lakes’ supply a delicate test
: and measurement of the land deformation. The important element
in the determination of the fact and of the amount of the deforma-
tion is the identity of the shore line or water level. In far separated
localities this may be in doubt but in the region described in this
writing the continuous tracing of the beaches leaves no uncertainty.

In calculating the amount of deformation in our district some
‘care 1s necessary, for several reasons: first, because the amount of
deformation is small; second, because the shore features are
variable; third, possible discontinuity of the water planes [see p.70];
fourth, errors in railroad or other data. The best data for fixing
the water levels are the crests of the wave-built gravel bars. Un-
doubtedly these are variable within narrow limits, some having
been formed higher than the lake surface and some lower, or
submerged. The higher and stronger and coarser of the marginal
bars may be safely regarded as overtopping the water by a few
(perhaps 5) feet. The lower bars in each cross-section were sub-
merged an uncertain and variable depth and are not reliable data,
at least for short distances. The stronger and higher marginal bars
are more reliable criteria, and in long distances their variations may

be neglected.

By using the Whittlesey and the stronger upper Warren bars
in our calculations it is found that the average amount of differential
uplift in our district is less than 2 feet a mile, but that the amount
of tilting a mile increases as we pass to the northeast. The facts
are given quantitatively in the following statement.

DEFORMATION IN NORTHEAST DIRECTION, USING WHITTLESEY BEACHES

From State Line to Marilla, 905—783 feet—=122 feet, +74 miles—1.64 feet
rise a mile

State Line to North Collins, 850—783==67 feet, + 48 miles—1.4 feet a mile

State Line to Fredonia, 820—783==37 feet, + 26 miles==1.4 feet a mile

Fredonia to North Collins, 850 —820==30 feet, + 22 miles—1.4 feet a mile

North Collins to Marilla, 905—-850==55 feet, + 26 miles 2.1 feet a mile

DEFORMATION IN NORTHEAST DIRECTION, USING WARREN BEACHES
State Line to “Pond” Survey station, 887—738—149 feet, + 92.5 miles—=
1.61 feet a mile
State Line to north of Marilla, 860—738—122 feet, + 75 miles=1.63 feet a
- mile
Westfield to ‘‘Pond” Survey station, 887—753—=134 feet, + 81 miles—=1.65
feet a mile ;
Westfield to Fredonia, 770—753=17 feet, + 15 miles==1.1 feet a mile
‘Fredonia to Hamburg, 807——770==37 feet, + 31 miles=1.2 feet a mile
Hamburg to Crittenden, 858—807==51 feet, + 24 miles= 2.1 feet a mile
Crittenden to “‘Pond Survey”’ station, 887—-858—29 feet, + 11 miles=2.6
feet a mile i

78 NEW YORK STATE MUSEUM a

The increasing rate of uplift as we proceed northeast is clearly
shown above, and is in entire harmony with facts in other portions ©
of the basin of the Great Lakes. Leverett has shown [Joc. cit.
Pp. 755] that for 200 miles west from Ashtabula, O., the Whittlesey
shore has practically no variation in altitudes, while east from
Ashtabula to New York the uplift is a little less than one foot a ©
mile. Farther northward in the Great Lakes basin the uplift is ;
more rapid than any rate in our district, the gradient east of Lake 4
Ontario being about 6 feet a mile. In the study of the beaches of |
Lake Iroquois along the north shore of Lake Ontario’ Professor Cole-
man finds that the rate of deformation is greatest in a line 20° east —
of north, and that it increases northward, being 2 feet a mile from _
Hamilton to York, 3.4 feet a mile from York to near Port Hope, —
and 4.17 feet a mile from the latter point to West Huntington. |

Using Professor Coleman’s isobase of west 20° north by east _
20° south we find that the Hamilton-York section of the Iroquois
shore corresponds in position of deformation with our Crittenden- —
Pond section of the Warren shore, and that the gradients are 2 and
2.6 feet a mile. The correspondence is sufficiently close to indicate —
that a large area is involved in the same deformation. |

The increase in elevation along these New York shore lines ©
toward the northeast dces not represent the full deformation of ©
the area. The direction of greatest uplift of certain beaches about ©
the upper Great Lakes has been found by Taylor to.lie along a line —
247° east of north, while in central New York it is believed that —
the line of maximum deformation is more nearly north and south |
or even west of north by east of south. As the direction of our —
shore line is about 45° east of north it follows that the maximum |
deformation of the region is somewhat greater than is indicated by ©
the beaches. _ |

The only north and south direction of any beaches in our district |
is the Whittlesey shore from Gowanda north to North Collins. ©
In the 5.5 miles south from North Collins to the residence of Mr _
B. W. Law there is a fall of 11 feet, or at the rate of 2 feet a mile, ‘
while the gradient southwest from North Collins to near Smiths ©
Mills is only 1.4 feet a mile. This comparison is only suggestive, |
as the distances are short and even a slight variation or error would |
make a disproportionately large difference in the result. A

The general uniformity in vertical distance including the several
bars of the two shores seems to prove that there was small deforma-
tion of tilting of the region during the life of the lakes [see p. osh|

Coleman, A. P., The Iroquois Beach in Ontario. Geol. Soc. Am_ Bul. |
1904. 15: 347-68. : ’

3
|

GLACIAL WATERS IN THE LAKE ERIE BASIN 79

If such canting had been in rapid progress during the existence of

the lakes the beaches should draw apart toward the northeast, or
in other words the vertical spacing between the earlier and later
beaches would increase to the northward. As there is an absence
of apparent increase in the spacing the only conclusion is that the
_ deformation of the region, or at least the tilting, has mostly occurred

| since the extinction of the lakes.

DELTAS AND LAKE PLAINS
These are features which mark the junction of stream and lake,

_ the product of the reaction of the drainage and the standing waters.

They are not so conspicuous locally as the beaches, but more
widespread, and of great geographic and economic importance.
The larger number of the villages of the district under description
have had their locations determined by these detrital plains. Along
the slopes nearer Lake Erie these gravel plains fronting the beaches
are the favored ground for the grape industry which characterizes
this part of the State. In the maps the deltas are not fully shown,
because the determination of their limits would require careful
survey and consume more time than was available.

Deltas of glacial drainage

It was inevitable that all drainage past the ice front should event -
ually reach standing water and deposit its burden of detritus. This

fact explains the origin of a great number of areas of sand and

gravel along the shore of the glacial lakes, some of them being of
great extent. We will briefly note the more important of these

deltas in order from west to east, or in the order of their formation.

As far east as Hamburg or East Aurora the deltas of this class are
related only to the Whittlesey waters, while from Marilla eastward
they correlate only with the Warren waters.

The lake bars or ridges of sand and gravel which may or may not
carry “Ridge roads” will be stronger and more developed every
way in the localities where detritus from drainage was concentrated.
From State Line to Westfield there was no very heavy accumula-
tion of delta material, the largest being in the region of Forsyth,
by the latest streams past the ice front from the eastward. All

the earlier drainage past the ice escaped on the landward side of

the Escarpment moraine and helped to build the delta plain west

of State Line.

Westfield. Some part of the material forming the detrital plain

on which the village stands must have been contributed by the
-drainage which cut the channels to the east and northeast.

SO NEW YORK STATE MUSEUM

Portland. We have here a clear example of a delta deposit
wholly by glacial drainage. As no large land stream enters here

the great detrital plain which is a mile wide at Portland and stretches © |
southwest for 3 miles was entirely the work of glacial rivers, specially ~
the great river which cut the remarkable channel, 8 miles long, 4

heading at Wheelers Gulf 3 miles south of Fredonia.

Lamberton. The sand deposits south of the village and extend-
ing toward Brocton were partly built by the lower streams on the
slope south of Fredonia.

Laona. The conspicuous terraces on the valley slope west of —

the village [see p. 21] are clearly the delta of the high-level rivers
from the northeast.

Fredonia. The upper part of the valley filling, or south of the
town, is partly the product of the later ice drainage on the lower
slope east of the town.

Northeast of Fredonia for 3 miles the bars are heavy, the material
being swept in by the later drainage on the slopes south of Sheridan.

Forestville. The village stands at the head of a delta which
extends 5 miles north, to Silver Creek. The work of the ice drain-
age and of Walnut creek has been combined here. The capacious
channels in the direction of Smiths Mills must have brought in a
large volume of detritus, and the ancient valley north of Forestville
may be deeply buried.

Gowanda. Some of the detrital filling in the Cattaraugus valley
was contributed by the ice drainage on the slope east and south
of North Collins.

Brant. The sand area at Brant is so extensive that it suggests a
delta deposit, but it is so far removed from the area of drainage that

its correlation is not clear. It may in part form an extension of

the sand area west of North Collins, and be derived from the
drainage past Eden.

Eden. The sand area west and northwest of Eden, and at Eden
Valley, would appear to be a delta produced by the streams on the
slope south of Hamburg.

Hamburg. The delta plain at Hamburg must have been partly:
the product of the glacial drainage on the northeast, or south of

Orchard Park.

East Aurora. The plain on which the village stands was built in
glacial waters, either Whittlesey or earlier local waters, by drainage
from the northeast.

East Elma. The plain northeast of the village was built in the

glacial waters by the several streams which cut across the moraine

from the east. This plain may have been the latest delta filling

. oe ee

GLACIAL WATERS IN THE LAKE ERIE BASIN 81

that was built wholly in Whittlesey waters. Other fillings up the

creek toward Porterville and Wales Center had similar origin.

Marilla. The valley filling at Marilla and farther up the valley
of Little Buffalo creek were contributed by the glacial drainage
from the east, but apparently at the Warren level. This would
seem to have been the earliest of the glacial stream deltas to form
at Warren level.

Cowlesville. The filling in Cayuga creek valley at and below
Cowlesville was carried in by the glacial streams which cut across
from the Attica (Tonawanda) valley on the east. This delta was
probably at first in local waters held higher than the Warren.

West Alden and Alden. The extensive sand areas forming the
bars at the Aldens were laid down in Lake Warren by the glacial
overflow from the Tonawanda valley along the line of the Erie
Railroad and past Darien.

Fargo. The extensive gravel plain south and southwest of Fargo
station on the Delaware, Lackawanna & Western Railroad was
wholly deposited by the glacial drainage from the east along the
course of the railroad.

Batavia. The plain on which the village stands is a detrital
filling and perhaps leveling of morainal gravels in shallow waters
of the Tonawanda valley. The drainage was across from the
Oatka valley, bringing the overflow of the Genesee valley and
other eastern valleys [see p. 31].

Deltas of land-stream drainage; existing streams

The deltas of this class were formed at any or at all levels in the
valleys in which were standing waters receiving contributions from
land drainage. Theoretically this drainage had no relation to the
ice front, and is in continued existence today. But practically
the deposits contributed by these land streams can not be always
discriminated from the same work in the same locality by the
glacial drainage. The two classes of streams were at work together,
and when a valley was receiving detritus from both glacial and
land drainage we should expect that the bulk from the latter source
would be dropped at the head of the bay, or wherever the land
stream had its mouth. When the glacial drainage ceased, the
land stream had no rival and was at liberty to spread its detritus
over all the delta area. We should regard the land stream detritus
as constituting the up valley portion and the superficial part of
many deltas, with variations depending, however, on the local
conditions.

82. NEW YORK STATE MUSEUM

In the Whittlesey territory no glacial drainage fell below the
Whittlesey level; therefore all detrital plains below Whittlesey
level in the Whittlesey area must correlate with land stream
drainage. The same must be true of all deposits below the Warren ~
level everywhere. But the materials of the lower land stream —
deposits were partly, in many cases, brought within the grasp of
the land stream by the glacial drainage.

In most valleys of the region detrital filling occurred at various
levels; in local glacial lakes, and at different hights; in Lake Whit-
tlesey; in Lake Warren; and in hypo-Warren waters. We shall —
note only a few of the more important delta plains which have
some relationship to the land stream drainage.

Westfield. The work of Chautauqua creek; in both Whittlesey ’

’ and Warren waters, and lower

Fredonia. Work of Canadaway creek; in the Shumla lake,
and in Whittlesey and Warren
Forestville. Work of Walnut creek; in local glacial lake, andin ~
Whittlesey
Hanover Center, Work of Walnut and Silver creeks; in Lake
Warren and lower
Gowanda. Work of Cattaraugus creek; the Fourmile evel in @
Whittlesey, the Versailles in Warren |
Pontiac. Work of Big Sister creek; in Warned and hypo-
Warren
Evans. Work of Big Sister and Little Sister creeks; in Dana
water :
Eden Valley. Work of south fork of Bightcenmile creek; in @
Whittlesey and Warren waters
North Boston. Work of Eighteenmile creek: in Whittlesey
water
Hamburg. Work of Eighteenmile creek; in Warren water
North Evans. Work of Eighteenmile creek; in hypo-Warren
waters : )
East Aurora. Work of Cazenovia creek; in local glacial water ;
and Whittlesey < ey.
Spring Brook. Work of Oe creek; in Lake Warren
Wales Center. Work of Buffalo creek; in local glacial (Porter- |
ville) lake .
Steitz Corners. Work of Buffalo creek; in Lake Warren
Marilla. Work of Little Buffalo creek; in Lake Warren
Cowlesville. Work of Cayuga creek; in local glacial lake 5
West Alden. Work of Cayuga aaa Ellicott creeks; in ‘Lake —
Warren ;

GLACIAL WATERS IN THE LAKE ERIE BASIN 83

Alden. Work of Ellicott creek; in Lake Warren
Attica. Work of Tonawanda creek; in local glacial (Attica)
lake
- Batavia. Work of Tonawanda creek; in local glacial waters
Indian Falls. Work of Tonawanda creek; in Lake Warren

TN DEX

Albion moraine, 14.

Alden, delta plain, 81, 83.

Alden moraine, 14.

Area described, 7.

Arkona beach, 42, 45.

Attica, Cowlesville to, 29-31;
plain, 83.

Attica lake, 30, 39, 40.

delta

Barre moraine, 14..

Base levels, two sets, 9.

Batavia, Cowlesville to, 29-31; over-
flow at, 31; delta plain, 81, 83.

Batavia channels, 4o.

Batavia moraine, 14.

Beaches, general description, 44-46.

Bear lake valley, outlet at head of, 18.

Belmore beaches, 42.

Bennington corners, 29.

Bibliography, 6-7.

Big {Inlet pass, 18.

Bishop, Irving P., cited, 6.

Boston lake, 36.

Brant, delta plain, 80.

Buffalo creek, 26.

Canadaway valley, glacial lake in, 37.

Caimllll, J. 15, Gadel, 6.

Cassadaga creek valley, 16.

Cattaraugus embayment,
19-23; east Of, 23—3 1.

Cattaraugus lake, 22.

Cattaraugus valley, 8, 34.

Cayuga creek, 26.

Cayuga valley, glacial waters, 36.

Cazenovia creek, 26.

Cazenovia valley, 57-59.

Chamberlin, T. C., cited, 6.

Channels, glacial drainage, 15-33;
carrying water from Erie basin,
16; conveying tributary water
from Oatka and Genesee valleys,
32-33. See also names of places.

Chautauqua creek, 17.

Chautauqua lake, swamp in big inlet,
iS),

Claypole, E. W., cited, 6.

Cleveland moraine, 12.

Coleman, A. P., cited, 78.
Conewango creek, cols at heads of
three branches, 18; valley, 16.
Cowlesville, East Aurora to, 25-29;

to Attica and Batavia,
delta plain, 81, 82.
Crittenden, West Alden to, 61-64.

west of,

Dana, lake, 43-44; beaches, 74-76.
Deltas,
79-81;

of land-stream drainage,
81—-83.=, a es pre) Bae

29-31; |

79-83; of glacial .drainage,

Divide, across main to Allegany
drainage, 16-18.

Drainage, Io-Il.

Dryer, C. R., cited, 41; investiga-
tions, 41.

East Aurora, 26; Hamburg to, 25; to
Cowlesville, 25-29; delta plain, 80,
82.

East Bethany, 32.

East Elma delta plain, 27, 80-81.

Eden, 24; delta plain, 8o.

Eden Valley, delta plain, 82.

Edson, Obed, cited, 6.

Erian ice lobe. diagram, 12.

Erie basin, 9.

Erie county, glacial lakes, 35.

Escarpment moraine, 13, 19.

Evans, delta plain, 82.

Fairchild, H. L., cited, 6-7.
Fargo, West Alden to, 61-64: delta
plain, 81.

Farrington Hollow glacial lake,
r8.

Forest beach, 45.

Forestville, Fredonia to, 21-22; to

Gowanda, 22-23; delta plain, 80,
82.

Forestville moraine, 13.

Fredonia, col south of, 18; Portland
to, 20-21, 52-53; to Forestville,
21-22; to Walnutand Silver creeks,
53; delta plain, 80, 82.

Genesee glacial lakes, outlet of
seventh stage of, 33.

Genesee outlets, 16.

Genesee valley, channels conveying
tributary water from, 32-33.

-Geography, 8-9.
WaGaliver ta Gayikers

cited, 7; investiga-
tions, 41.
Glacial drainage,
deltas of, 79-81.
Glacial history, outline of, g—11.
Glacial lakes, local, 33-38; with
outlet to southern drainage, 34-36;
with outlets past the ice front, 36—
38; in valleys east of the Tona-
wanda creek, 40-41; greater, 4I—

channels, 15-33;

44.

Glenwood-Colden lake, 36.

Gowanda, Forestville to, 22-23; to

' Hamburg, 23-25; Hanover Center
to, 54-55; to North Collins, 55-56
delta plain, 80, 82.

Gowanda moraine, 13, 26.

Gowanda planes, outlets, 38-39.

Gowanda, valley, water levels, 37.

86

Greater glacial lakes, 41-44; shore
lines, 44-68.

Gulf, gullies leading eastward, 19.

Hall, James, cited, 7.

Hamburg, Gowanda to, 23-25; to
East Aurora, 25; North Collins to,
56-57; to Spring Brook, 57-59;
delta plain, 80, 82.

Hamburg moraine, 13-14, 26.

Hanover Center, to Gowanda, 54-55
delta plain, 82.

Humphrey Hollow lake, 29.

Ice body, relation to general land
surface, 16-18.

Ice margins, II-I5.

Indian Falls, delta plain, 83.

Java-Wales lake, 36.

Lake Escarpment moraine,

Lake plains, 79-83.

Lake waters, II.

Lakes, see also names of lakes.

Lafiiberton, delta plain, 80.

Land surface, relation of ice body to,
16.

Land warping, 76-79.

Laona, delta plain, 80.

Law, B. W., acknowledgments to,
Dey mentioned, 38.

Leverett, Frank, studies of, 5; cited,
Gig Ebsic: U[Se investigations, 4t.

Little Buffalo creek, 26.

Little Inlet creek, col at head Oi, Wy.

Local glacial lakes, 28-30:

if Zo

Machias, outlet, 16.
Machias stage, 35.
Maps, 7

Marilla, 27; delta plain, 28, 81, 82.

Marilla moraine, 14, 26.

Maumee, lake, 41-42.

Moraines, 11-15; interpretation of,
26,

New Oregon-Clarksburg lake, 35.
Newberry, J. 5., cited, 7; investiga-
TOMS a eee

Newberry lake, 32.

Newberry plane, 40.

North Boston, delta plain, 82.

56; to Hamburg, 50-57.
North Evans, delta plain, 82.
North Java lake, 39.

Oatka valley, channels conveying
tributary waters from, 32-33.

Pembroke ridges; 14.

Persia flag station, channel, 17.
Persia outlet, 22, 35..

Persia stage, 35.

North Collins, 24; Gowanda to, 55— |

| Whittlesey, lake, 42-43; beach,
| Whittlesey level,

74-
Williston, 218.7) aie

INDEX

Pontiac, delta plain, 82.

Portland, Westfield to, 20, 50-52: tomy
Fredonia, 20-21, 52-53; delta
plain, 80.

Protection-Holland lake, 36.

Recessional moraines, 11.
Ripley, channel near, 19.

Scourways, 24.

Shore lines of the greater lakes, 44— _
68; deformation of, 76—79.

Shumla lakes; armen

Silver creek, Fredonia to, 53; to
Gowanda, 54-55.
Spencer, J. W., cited, 7, 42) 45 ;sum-

vestigations, 41.

Spring Brook, Hamburg to, 57-59;
to West Alden, 59-61; delta plain,
82.

State Line to Westfield, 46-50.

Steitz Corners, delta plain, 82.

Tarr, R. S., cited, 7.

Taylor, Frank Bi.) eitedyajessen
investigations, 41.

Terminal moraine, II.

Tonawanda creek, 31

Tonawanda valley, glacial lakes, 36,
39-40.

Tonawanda waters, 30.

Topography, 8-9.

Twentymile creek, 19.

Tt;

Upham, Warren, cited, 7.

Varysburg-Johnsonburg lake, 29, 36,
39:

Wales Center, delta plain, 82.
Walnut creek, Fredonia to, 53.
Walnut lake, 18, 22, 37.

Warren, lake, 433 beach, 20, 455 46—
64.

Warren level, discussion of, 64—74.

Warren Tributary lake, 33.

Warsaw lake, 4o.

West Alden, Spring Brook to, 59-61;
to Crittenden, 61-64; to Fargo
Station, 61-64; delta plain, 81,82.

Westfield, to Portland, -20, 50-52;
Bee Line. to, 46-50; delta plain,

79
wheeien' s gulf, ar.
2c,
45, 46-64.
discussion of, 64- —

Winchell, N. ‘investigations, 41;
cited, 42.
Wisconsin ice sheet, Ir.

Wyoming county, glacial lakes, ese.

Hes

_ Wyoming Pavilion) lake, 4I..

me New York State Education Department

New York State Museum
Joun M. CiarkeE, Director

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En18 (68) Needham, J. G. & others. Aquatic Insects in New York. 322p.
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Enrg (72) Felt, E. P. Grapevine Root Worm. 58p. 13pl. Nov. 1903. 20¢.

Tis is a revision of En1r6 containing the more essential facts observed since that was pre-

pared.

En20 (74) & Joutel, L. H. Monograph of the Genus Saperda. 88p.
14pl. June 1904. 25¢.

En2ir (76) Felt, E. P. roth Report of the State Entomologist 1903. 15o0p.
4pl. 1904. I5¢.

Mosquitos or Culicidaeof New York. 164p.il. 57pl. Oct.

1904. 40.

En23 (86) Needham, J. G. & others. May Flies and Midges of New York.
352p. il. 37pl. June 1905. Soc, cloth.

En24 (97) Felt, E. P. 20th Report of the State Entomologist 1904. 246p.
il. ropl. Nov. 1905. 406.

En25 (103). Gipsy and Brown Tail Moths. 44p. ropl. July 1906. 15¢

En26 (104) —— 21st Report of the State Entomologist 1905. 144p. t1opl.
Aug: 1906. 25¢.

Needham, J. G. Monograph on Stone Flies. In preparation.

Botany. Bor (2) Peck, C. H. Contributions to the Botany of the State of
New York. 66p. 2pl. May 1887. Out of print.

Boz (8) Boleti of the United States. 96p. Sep. 1889. [soc]

Bo3 (25) —— Report of the State Botanist 1898. 76p. 5pl. Oct. 1899.
Out of print.

Bo4 (28) Plants of North Elba. 206p. map. June 1899. 206.

Bos (54) —— Report of the State Botanist rgo1. 58p.7pl. Nov.1g02. 4oe.

Bo6 (67) —— Report of the State Botanist 1902. 196p. 5pl. May 1903.
50¢.

Bo7 (75) —— Report of the State Botanist 1903. 7op. 4pl. 1904. 40¢.

Bo8 (94) —— Report of the State Botanist 1904. 6op. ropl. July 1905. 4oe.

Bog (105) —— Report of the State Botanist 1905. 1108p. 12pl. Aug.

1996. 506

ecae ology. Arr (16) Beauchamp, W. M. Aboriginal Chipped Stone Im-
plements of New York. 86p. 23pl. Oct. 1897. 295c.

Ar2 (18) Polished Stone Articles used by the New York Aborigines.
104p. 35pl. Nov. 1897. 25c.

Ar3 (22) Earthenware of the New York Aborigines. 78p. 33pl. Oct.
1898. 25¢.
Ar4 (32) ——Aboriginal Occupation of New York. tg90p. r6pl. 2 maps,

lMar. 1900. 30c.

\

NEW YORK STATE EDUCATION DEPARTMENT

Ars (41)
166p. 28pl. Mar. 1901. 306.

Ar6 (50) Horn and Bone Implements of the New York Indians. 112p.
43pl. Mar. 1902. 30¢.

Ar7 (55) Metallic Implements of the New York Indians. o4p. 38pl.
June 1902. 25¢. eras

Ar8 (73) Metallic Ornaments of the New York Indians. 122p, 37pl.
Dec. 1903. 306.

Aro (78) History of the New York Iroquois. 340p. 17pl. map. Feb.
1905. 75¢, cloth.

Arto (87) Perch Lake Mounds. 84p. t12pl. Ap. 1905. 20¢.
Ari1 (89) Aboriginal Use of Wood in New York. t1gop. 35pl. June
1905. 356. ;

Beauchamp, W. M. Aboriginal Place Names of New York. In press.

—— Civil, Religious and Mourning Councils and Ceremonies of Adoption.
In press.

MSeelcabeUe. Msr (62) Merrill, F. J. H. Directory of Natural History
Museums in United States and-Canada. 236p. Ap. 1903. 306.

Ms2 (66) Ellis, Mary. Index to Publications of the New York State Nat-
ural History Survey and New York State Museum 1837-1902. 418p.
June 1903. 75¢, cloth.

Museum memoirs 1889—date. OQ.

1 Beecher, C. E. & Clarke, J. M. Development of Some Silurian Brachi-
opoda. g6p. Spl. Oct. 1889. $1.

2 Hall, James & Clarke, J. M. Paleozoic Reticulate Sponges. 35op. tl. 7opl.
1898. $1, cloth.

37 Clarkes alle M. The Oriskany Fauna of Becraft Mountain, Columbia Co.
NvYo s28puopl nOctimgoor. coc:

4 Peck,C.H. N.Y. Edible Fungi, 1895-99. 106p.25pl. Nov. zg00. 756.

This includes revised descriptions and illustrations of fungi reported in the 4oth, 51st and sod
reports of the State Botanist.

5 Clarke, J. M. & Ruedemann, Rudolf. Guelph Formation and Fauna of
New York State. 196p. 21pl. July 1903. $1.50, cloth.

6 Cle J. M. Naples Fauna in Western New York. 268p. 26pl. map.
$2, cloth.

7 Ruedemann, Rudolf. Graptolites of New York. Pt 1 Graptolites of the
Lower Beds. 350p.17pl. Feb.1905. $1.50, cloth.

8 Felt, E. P. Insects Affecting Park and Woodland Trees. v.1 46op. il.
48pl. Feb. 1906. $2.50, cloth. v.2 In press.

9 Clarke, J. M. Early Devonic of New York and Eastern North America,
In press.

Io Soa C. R. The Devonic Fishes of the New York Formations.

Ww press.
Eaton, E. H. Birds of New York. In preparation.

Ruedemann, R. Graptolites of New York. Pt 2 Graptolites of the Higher.

Beds. In preparation.

Natural history of New York. 3ov. il. pl. maps. Q. Albany 1842-94.

DIVISION 1 zooLOGY. De Kay, James E. Zoology of New York; or, The
New. York Fauna; comprising detailed descriptions of all the animals
hitherto observed within the State of New York with brief notices of
those occasionally found near its borders, and accompanied by appropri-
ate illustrations. 5v.il.pl.maps. sq.Q. Albany 1842-44. Out of print.
Historical introduction to the series by Gov. W. H. Seward. 178p.

v. 1 ptr Mammalia. 131+ 46p. 33pl. 1842.
300 copies with hand-colored plates.
v. 2 pt2 Birds. 312+380p. 14ipl. 1844.

: Colored plates. Pow

v. 3 pt3 Reptiles and Amphibia. 7+98p. pt4 Fishes. 15+415p. 1842.
pt3—-4 bound together.

v. 4 Plates to-accompany v. 3. Reptiles and Amphibia 23pl. Fishes 7gpl.
1842.
300 copies with hand-colored plates.

v. 5 pt5 Mollusca. 4+271p. gopl. pt6 Crustacea. 7op. 13pl. 1843-44.
Hand-colored plates: pts—6 bound together. ;

Wampum and Shell Articles used by New York Indians.

MUSEUM PUBLICATIONS

DIVISION 2 BOTANY. Torrey, John. Flora of the State of New York; com-
prising full descriptions of all the indigenous and naturalized plants hith-
erto discovered in the State, with remarks on their economical and medical
properties. 2v.il.pl.sq.Q. Albany 1843. Out of print.

vy. « Flora of the State of New York. 12+484p. 72pl. 1843.

300 copies with hand-colored plates.

v. 2 Flora of the State of New York. 572p. 89pl. 1843.
300 copies with hand-colored plates.

DIVISION 3 MINERALOGY. Beck, Lewis C. Mineralogy of New York; com-
prising detailed descriptions of the minerals hitherto found in the State
of New York, and notices of their uses in the arts and agriculture. il. pl.
sq.Q. Albany 1842. Out of print.

v. 1 ptr Economical Mineralogy. pt2 Descriptive Mineralogy. 24+536p.
1842.

8 plates additional to those printed as part of the text.
DIVISION 4 GEOLOGY. Mather, W. W.; Emmons, Ebenezer; Vanuxem, Lard-
ner & Hall, James. Geology of New York. qv. il. pl. sq. Q. Albanv
1842-43. Out of print.

.1 ptr Mather, W.W. First Geological District. 37+653p. 46pl. 1843.

2 pt2 Emmons, Ebenezer. Second Geological District. 10+437p. 17pl.

1842. °

. 3 pt3 Vanuxem, Lardner. Third Geological District. 306p. 1842.

. 4 pt4 Hall, James. Fourth Geological District. 22+4683p. i19pl. map.

1843.

DIVISION 5 AGRICULTURE. Emmons, Ebenezer. Agriculture of New York;
comprising an account of the classification, composition and distribution
of the soils and rocks and the natural waters of the different geological
formations, together with a condensed view of the meteorology and agri-
aa productions of the State. 5v.il. pl.sq.Q. Albany 1846-54. Out
of prent.

v. 1 Soils of the State, their Composition and Distribution. 11 +371p. 21pl.
1846.

v. 2 Analysis of Soils, Plants, Cereals, etc. 8+343+46p. 42pl. 1849.
With hand-colored plates.

v.3 Fruits, etc. 8+340p. 1851.

v.4 Plates to accompany v. 3. g5pl. 1851.

Hand-colored.

v. 5 Insects Injurious to Agriculture. 8+272p. Sopl. 1854.
With hand-colored plates. : .

DIVISION 6 PALEONTOLOGY. Hall, James. Palaeontology of New York. 8v.
il. pl.sq.Q. Albany 1847-94. Bound in cloth.

v. 1 Organic Remains of the Lower Division of the New York System.
23+338p. oopl. 1847. Out of print.

v. 2 Organic Remains of Lower Middle Division of the New York System.
8+362p. to4pl. 1852. Out of print.

v. 3 Organic Remains of the Lower Helderberg Group and the Oriskany
Sandstone. pti, text. 12+532p. 1859. [$3.50]

pt2. 143pl. 1861. [$2.50]

_v. 4 Fossil Brachiopoda of the Upper Helderberg, Hamilton, Portage and
Chemung Groups. 11+1+428p. 69pl. 1867. $2.50.

v. 5 pti Lamellibranchiata 1. Monomyaria of the Upper Helderberg,

. Hamilton and Chemung Groups. 18+268p. 45pl. 1884. $2.50.

Lamellibranchiata 2. Dimyaria of the Upper Helderberg, Ham-
ilton, Portage and Chemung Groups. 62+293p. 51pl. 1885. $2.50.

—— pt2 Gasteropoda, Pteropoda and Cephalopoda of the Upper Helder-
berg, Hamilton, Portage and Chemung Groups. zv. 1879. v. 1, text.
15+492p. v. 2, 120pl. $2.50 for 2 v.

& Simpson, George B. v. 6 Corals and Bryozoa of the Lower and

Upper Helderberg and Hamilton Groups. 24+298p. 67pl. 1887. $2.50.

& Clarke, John M. v. 7 Trilobites and other Crustacea of the Oris-

kany, Upper Helderberg, Hamilton, Portage, Chemung and Catskill

Groups. 64+236p. 46pl. 1888.:*\Cont. supplement to v. 5, pt2z. Pterop-

oda, Cephalopoda and Annelida.““42p. 18pl. 1888. $2.50.

pied

<<

|

tu

a ee Th en

PLATE 1
General map showing ancient lake shores and

abandoned stream channels in the New York
part of the Erie basin

PLATE 2

Effects of glacial waters, State Line to Sheridan

PLATE 3

“Effects of glacial waters, Sheridan to Gowanda

PLATE 4

Effects of glacial waters, Gowanda to Orchard Park

PLATE 5

Work of glacial waters, Orchard Park to Batavia

PLATE 6

Glacial stream channels, Attica to Genesee Valley

NEW YORK STATE EDUCATION —————

& Clarke, John M. v. 8 ate Introduction to the Study of the on

of the Paleozoic Aree 16+367p. 44pl. 1892. $2.50. a

& Clarke, John M. 8 pt2 Paleozoic Brachiopoda. 16+ 394p. 64
1894. $2.50. :

Catalogue of the Cabinet of Natural History of the State of New York and
of the Historical and Antiquarian Collection annexed thereto. 242p. O.
1853.

Handbooks 1893-date. 74x124 cm.

In quantities, 1 cent for each 16 pages or less. Single copies postpaid as below.

New York State Museum. 52p. il. 4c.

Outlines history and work of the museum with list of staff 1902.

Paleontology. 12p. 2¢. :
Brief outline of State Museum work in ale ontciaey under heads: Definition; Relation tal '

biology; Relation to stratigraphy; History of paleontology in New York. y

Guide to Excursions in the Fossiliferous Rocks of New York. t124p. S¢.~
Itineraries of 32 trips covering nearly the entire series of Paleozoic rocks, prepared specially

tor the use of teachers and students desiring to acquaint themselves more intimately with the —

classic rocks of this State. q

Entomology. 16p. 2c.

Economic Geology. 44p. 4¢.

Insecticides and Fungicides. 20p. 3c.

Classification of New York Series of Geologic Formations. 32p. 3c.

Geologic maps. Merrill, F. J. H. Economic and Geologic Map of the State
of New York; issued as part of Museum bulletin 15 and 48th Museum
Report, v. 1. 59x67 cm. 1894. Scale 14 miles to 1 inch. 145¢. :

—— Map of the State of New York Showing the Location of Quarries of

Stone Used for Building and Road Metal. Mus. bul. 17. 1897. 0c. ~

—— Map of the State of New York Showing the Distribution of the Rocks —
Most Useful for Road Metal. Mus. bul. 17. 1897. 5c. a

—— Geologic Map of New York. 1901. Scale 5 miles to 1 inch. In atlas”
form $3; mounted on rollers $5. Lower Hudson sheet 60c. .

The lower Hudson sheet, geologically colored, comprises Rockland, Orange, Dutchess, Put-~
nam, Westchester, New York, Richmond, Kings, Queens and Nassau counties, and parts of Sul- —
livan, Ulster and Suffolk counties; also northeastern New Jersey and part of western Connecticut

—— Map of New York Showing the Surface Configuration and Water Sheds.
TOOL = Seale izemmileseto rT aineh. 756: ;

Map of the State of New York Showing the Location of its Economic

Deposits. 1904. Scale 12 miles. to 1 inch. 145c. 3

Geologic maps on the United States Geological Survey topographic base;
scale 1 in. = 1m. Those marked with an asterisk have also been pub-
lished separately. q

*Albany county. Mus. rep’t 49, v. 2. 1898. 5o0c.

Area around Lake Placid. Mus. bul. 21. 1808.

Vicinity of Frankfort Hill [parts of Herkimer and Oneida counties]. Mus.
KO) b Sies Wo Wa | USO).

Rockland county. State geol. rep’t 18. 1899.

Amsterdam quadrangle. Mus. bul. 34. 1g00.

*Parts of Albany and Rensselaer counties. Mus. bul. 42. Igor. 406.

*Niagara river. Mus. bul. 45. rg01. 256.

Part of Clinton county. State geol. rep’t 19. Igor. i

Oyster Bay and Hempstead quadrangles on Long Island. Mus. bul. 48.
Igol. q

Poutisne of Clinton and Essex counties. Mus. bul. 52. 1902. :

Part of town of Northumberland, Saratoga co. State geol. rep’t 21. 19934

Union Springs, Cayuga county and vicinity. Mus. bul. 69. 1903.

*Olean quadrangle. Mus. bul. 69. 1903. Joc. q

*Becraft \Mt with 2 sheets of sections. (Scale 1 in. $m.) Mus. bul. ‘Gg aH
1903. )20C.

*Canandaigua-Naples neadeeraie. Mus. bul. 63. 1904. 206.

*little Falls quadrangle. Mus. bul. 77. 1905. Tr5c.

*Watkins-Elmira quadrangles. Mus. bul. 81. 1905. 206.

“Tully quadrangle. Mus. bul: 82. 1905. 106.

*Salamanca quadrangle. Mus. bul. 80. 1905. Troe.

*Buftalo quadrangle. Mus. bul. 99. 1906. Toc.

*Penn Yan—Hammondsport quadrangles. Mus. bul. ror. 1906. 206,

4

BULLETIN 106 PLATE 1

STATE MUSEUM

M CLARKE

EDUCATION DEPARTMENT voxn

LEGEND

XSLT
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be RSG g
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H. L. Fairchild 1905

THE NEW YORK PART OF THE ERIE BASIN

GENERAL MAP SHOWING ANCIENT LAKE SHORES AND ABANDONED STREAM CHANNELS IN

—o

EDUCATION DEPARTMENT
JOHN M CLARKE
STATE GEOLOGIST

UniyeRSITY OF THE STATE OF NEW YORK.

STATE MUSEUM BULLETIN 106 PLATE 2

WESTFIELD. DUNKIRK QUADRANGLES

‘me 35° 7380" S 2
30 f
| Seale aztoo
| pee SE 2 A 4 j Kilometers
H b |

Contour interval 20 fret
Datu in rican eis Teva

Van Buren Pt pK.

Beaches of Lake
Warren and
lower waters

= :

Beach of Lake \ \
Whittlesey
Mme] Both banks
preserved
Only one bank
now existing Fy
d v
Hypothetical, or \ é
M) unezaminedt .
@iaoial Stream g
channels 5
S

F-=-4 | se

Divide between
Erie and

Allegany waters bs

HL. Fairchild i905

EFFECTS OF GLACIAL WATERS, STATE LINE TO SHERIDAN

“we

EDUCATION DEPARTMENT UNIVERSITY OF THE STATE OF NEW YORK

JOHN M CLARKE - y Tm
STATE GEOLOGIST STATE MUSEUM

BULLETIN j06 PLATE 3
PARTS OF SILVER CREEK AND CHERRY CREEK QUADRANGLES

RTL

Ze. >

\\)\)

EFFECTS OF GLACIAL WATERS,
SHERIDAN TO GOWANDA

HL. Fairchild 1905

LEGEND

Hoaches of Lake
‘@rren and
lower waters

|

Bench of Lake
Whittlesoy

G)actal Stream
channels

Moraine

Delta

Divide between
Erle and
Allegany waters

Gow

vei

os ace.” 3. oe i = ae as ee a ee es a et sae = A. a my -
— EDUCATION DEPARTMENT . UNIVERSITY OF TH STATE OF NEW YORK zl the Ps i i ee ad ica ce
_ ‘ : STA : ie v

oS ——_ : AS eS ae ee Bo BULLETIN 105 PLATE 4

eee
aay

>

we |

S— Ei nes

RI castes Be
Glacial Stream
chauniels

Lr 3
- =
EFFECTS OF GLACIAL WATERS, GOWANDA TO ORC ) PARK
; ; ; .
- a a. a, eee '

EDUCATION DEPARTMENT UNIVERSITY OP THE STATE OF NRW YORK
JOHN M CLARKE

STATE GKOLOOIST

STATE MUSEUM

BULLETIN 106 PLATE 5.
OF BUFFALO QUADRANGLES

ATTIGA, DEPEW AND PART

®
ef
3 }
pst
=

Lake Whittlose;

=

AW

&
a
4
2
i

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Mt
if

Li

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Pip

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=
Ware

ila 3 a

i

ili

HOLLOW hon

H. L, Fairchild igo5

WORK OF GLACIAL WATERS, ORCHARD PARK
TO BATAVIA ©

UNIVERSITY OF THE STATE OF NEW YORK
BULLETIN 106 PLATE 6
BATAVIA AND PART OF CALEDONIA QUADRANGLES

STATE MUSEUM

EDUCATION DEPARTMENT
0)

JOHN M CLARKE
STATE GEOLOGIST

Beaches of Lake
Warren and
lower waters

Both banka

preserved
‘Only one bank
| now erixtng

| Hypothetical, or
unexamined

Glacial Stream
channels

Balt IM LIT.
Fanaa NWORS Moraine
{
%

Delta
and
Alloviam

H. L. Fairchild igos

VTS
10°

GLACIAL STREAM CHANNELS,
ATTICA TO GENESERE VALLEY

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