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Published monthly by the

New York State Education Department

BULLETIN 408

JULY 1907

N eW York State Museum

Joun M, CLARKE, Timers

Bulletin 111

GEOLOGY 13

DRUMLINS OF

CENTRAL WESTERN NEW YORK

Inbroduction - general description 391
Pea eet MISE LION. 22.3.7... Ae
ONS GOT UO) Vain rr ie, 3QO

ee RR acl
ware Ls FAIRCHILD RANS
PAGE ; PAGE
Relation to moraines............ 424
204"), ‘Specialteathnes, tame... aoe eeedae
Syracuse island masses........ 425 .
402 Montezuma island groups..... 426

Relation to larger topography..
Relation to underlying rock strata 404

Nondrumlin areas: open spaces 426

Form and dimensions........... 405 Channels among the drumlins. 427
(0) GUS C0 en ATO) ie Stati iadar yas ote, eae Ges tiate'e oc 420
Composition and structure....... 412 Agee of the crim: . .s.hsa-ee 429

ao coscd) it 413 Thrust motion of the ground
Gomeenttic bedding;,. ¢s.0...... 416 WCOMtACHI Ces eee dics eee 429
Formation: theoretical mechanics 419 OPPS TAT peta aha Piette aa! caren 431
a Dynamic factors pertaining DD yrrainities’yatscpat oete oe ee uae 432
POMUME MECIDOUY sig. sic. socks 20 IDNs phanlshalaopmeas,; cela Meher na | ae 33

6 Factors relating” to the drift Depth of the drumlin-making
HGIGMIIIMENICE... 6 vce cs es os 421 LCOS nets & ftok t oR eee 434
¢ Factors of external control... 422 | Drumlins of Ireland es Gee eee at 435
Drumlin forms and observed Bib ln@emmarplany esto cs asd gthei. storne cues 436
121) 0) 2 CSA ae Ae RtoDe lie ere en eye taf tckeute devre 6 s,s lop aathe 441

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STATE OF NEW YORK .
EDUCATION DEPARTMENT

Regents of the University

of

With years when terms expire

WHITELAW Retp M.A. LL. oe Chancellor - -
Sr Craik McKetway M.A. LL. Dy Vice Chancellor
DANKE BrACcHt Pins ese ae Vege = 7) eee An ieee
Pusat (Suxrom eee ieee ul Gee igee
T. GuiLForp SmitH M.A. C.E. LL.D. Tee
Witittam NottTincHamM M.A. Ph.D. LL-D. -

CHARvES A.) GarRpDINER PhyDSl bap wLal sD Dace,

ALBERT VANDER VEER M.D. M.A. Ph.D. LL.D.
EDWARD» LAUTERBACH JNEJA MILA acme Me ht:
EucEne .A. Puirsin LL.B: LL.D. ite ae
LUGAN LL. ‘SHEDDEN* LALA B y= oye. er oe

Commissioner of Education

ANDREW S. DRAPER LL.B. LL.D.

Assistant: Commissioners

Howarp J. Rocers M.A. LL.D. First Assistant

-

| New York

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New Vork State Education Department
Sctence Division, October 19, 1906
Hon. Andrew S. Draper LL.D.
; Commissioner of Education
Sir: I communicate herewith, for publication as a bulletin of the
State Museum, an important. paper on the glacial phenomena of New
York, entitled the Drumlins of Central Western New York by Professor

eG. Pairehild, *
Very respectfully yours

Joun M. CLARKE
Director and State Geologist

Approved for publication October 20, 1906

Commissioner of Education

EDUCATION DEPARTMENT
JO; M. CLARKE
STATE GEOLOGIST

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New York State Education Department

New York State Museum

Joun M. Crarke, Director

Bulletin 111

GEOLOGY 13

DRUMLINS OF CENTRAL WESTERN NEW YORK

BY
H. L. FAIRCHILD

Introduction: general description

Among the varied products of glacial work the smooth mounds
and ridges known as drumlins are the most singular. They are the

product of continental glaciers by the unique rubbing or molding

action of the latter as plastic solids. In their form, attitude, compo-
sition and relation they are not only the most remarkable and inter-
esting of the glacial drift deposits but in their graceful outlines and
smooth surfaces they are the most striking and beautiful of drift
forms, ii not of all topographic forms of moderate size. Long
before the glacial origin of the drift was established these smooth-
outlined hills had attracted attention. They were cited as an objec-
tion to the theory of continental glaciation because they seemed
inconsistent with the supposed planing and leveling effect of the ice
sheet ; and even up to the present time they have remained some-
thing of a difficulty if not a puzzle. Although the subglacial origin
of the drumlins is generally admitted and their constructional genesis
conceded, at least in part, the precise mechanical operation in their
upbuilding by the antagonistic and balancing forces has not been
analyzed. Some of the factors in this complicated problem in
glacial mechanics will be indicated below.

The State of New York may claim with confidence the possession
of the most remarkable group of drumlins in the world, when all the
facts relating to them are taken into account. This drumlin area
has been under the writer’s observation for several years and

Seine results of the study will help, it is thought, to elucidate the

39f

3902 NEW YORK STATE MUSEUM

problem of drumlin formation. It is recognized that no single
drumlin area may exemplify all the features belonging to these
drift forms, but the New York area includes such a large variety of
forms and relationships that it should illustrate the fundamental
mechanics and most of the phenomena. ;

For the reader who may not be familiar with this form of the
glacial.drift a brief description of its general character will be
appropriate. ‘That these hills are of glacial origin is evident from
their location always within the glaciated territory, their superficial
position and their composition which is compact till or ground
moraine, at least in New York. Their molded forms show the over-
viding effect of the ice and they are believed to have been shaped, if
not constructed, under the relatively thin and weaker border of the
continental ice sheet, along the zone where the ice in its transport-
ing power became incompetent to carry further its drift burden.
Their forms vary from mounds to long, slender ridges; and their
size from massive, conspicuous hills, 100 or 200 feet high, to indefi-
nite swells of the drift surface. 7

The history of the earlier study of drumlins may be read in the
article by W. M. Davis, “Distribution and Origin of Drumlins”
[see p. 437]; and also in the papers by Warren Upham, specially
those of the years 1889, 1892 and 18093 [see p. 438]. A brief synopsis
of the description by Kinahan and Close of the type drumlins in
Ireland is appended as pages 435-36, with a copy of part of their
map [pl. 471. |

The following names were formerly applied to the drumlin forms:
parallel ridges, Sir James Hall, 1815 ; drumlins, H. M. Close, 1366;
parallel ridges, Shaler, 1870; lenticular hills, Hitchcock, 1876;
whalebacks, Matthew, 1877 ; drums and sowbacks, J. Geikie, 1877 ;
parallel drift hills, Johnson, 1882; mammillary and elliptical hills,
Chamberlin, 1883. |
The name “drumlin” (derived from the Celtic and meaning
“little hill’) was first applied by H. M. Close in 1866 to these drift
hills in Ireland. The various names formerly applied haye by
common consent given way to the present name, which was intro-
duced in this country by W. M. Davis in 1884 i

Drumlins are so diverse in their form, and possibly in their pre-
cise origin, that any terse definition must be somewhat vague. The
smooth form, convex profile and parallelism with the ice flow

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ORPOGRAPHY

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EDUCATION DEPARTMENT
JOHN M. CLARKE
STATE GEOLOGIST

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DRUMLINS OF CENTRAL WESTERN NEW YORK 2.203

direction are the striking superficial characters ; but along with these
elements ‘the composition and subglacial origin must be recog-
nized. Omitting reference to the precise manner of their amass-
ing, they may be defined as smooth-surfaced hills of till, elongated
in the direction of ice movement by the rubbing action of the ice
sheet. Or, more briefly, they may be defined as smooth drift hills
shaped by ice molding.

The topographic expression of drumlins is so emphatic that any
group with fairly developed forms is readily distinguished on maps
in 20 foot contours. Plate 3 affords a comparison of drumlinized

_ drift with other forms of glaciated topography.

It appears that the molding effect of the overriding ice was not
restricted to the drift masses deposited during the rubbing process
by the ice itself, but was felt by moraines or even by rock masses
which were exposed to the ice rubbing. The latter effect is seen
specially along the summits of the rock ridges that were buried under
the glacier [sce pl. 10]. The name drumlin can not appropriately
be applied to ice-shaped rock masses, though the relationship to
drumlins may be evident. The term “drumloid”’ is fully appropriate
but the word has long been used in-a rather loose and indefinite way
for hills of drift having merely a formal and perhaps accidental
resemblance to drumlins. A ‘distinctive term with obvious meaning
is desirable, and it is proposed to call these forms Rocdrumlins,

“using as a prefix the Celtic word for rock. In the case of ice-worn

hills or summits of rock which suggest the drumlin form but do not
fully attain it we may use the term rocdrumloid.

It should be emphasized that rocdrumlins are an effect of a
moderate amount of erosion, or the removal of material, while the
drumlins are a product of upbuilding and shaping at the same time
[see p.432] The genetic distinction is important.

It seems probable that hill summits of rock should receive under
favorable conditions a drumloid expression, that is, a roches.

-moutonné form on a large scale. Plate 16 shows quite as good an

example as the published topographic sheets of western New York

supply, and even this is somewhat equivocal. Eastern New York

can probably furnish better examples. However, it may be said
that the erosional work of the continental ice sheet was commonly
insufficient, at least in western New York, to strongly mold the hill-

tops. The absence of such effect 1s seen in plate 3, figure 1.

394 NEW YORK STATE MUSEUM

Areal distribution

Drumlins have an irregular and apparently capricious distribution
over the glaciated territory of Europe and America and over large
areas seem to be entirely wanting. None have been reported from
Ohio, Indiana, Illinois, Minnesota, the Dakotas, southern Michigan
and most of Iowa. They are at least very rare in Pennsylvania and
New Jersey. In Maine they are not infrequent but are inferior in
numbers and size to those found southwestward.

There seem to be three regions of great drumlin development in
the United States. The New England area includes southern New
Hampshire, where Upham has mapped nearly 700 drumlins ; Massa-
chusetts with 1800, as described by Barton; and a southward
extension of the area across Connecticut. The Michigan area
includes the eastern part of Wisconsin and adjacent territory in
Michigan, where Chamberlin estimates that there are 5000 drumlins ;
also east of the north end of Lake Michigan in the Grand Traverse
district. The third area is the subject of this paper.

Drumlins have been noted in the southern part of Canada by
G. F. Matthew, in Manitoba and Athabasca by J. B. Tyrrell, and are
said to occur in Nova Scotia.

The drumlins of Ireland are the type forms and are briefly described
at the close of this paper [». 435-36]. Drumlins also occur in
the Clyde valley in Scotland, and in the Lake Country of England
as described by Upham [titles for 1898, p. 439]. In the low grounds
of Switzerland they are said to occur; also in northern Germany on
the island of Rtigen and east of the lower part of the river Oder.
Dr Keilhack has described in the latter area a group of 3e00
drumlins.t They are said to be disposed radially, facing a looped
marginal moraine, covering a belt 6 by 20 to 4o miles.

In Scandinavia drumlins have escaped notice, unless certain clay
ridges in Sweden, noted by James Geikie,? represent drumlinized
surface. eat

When it is recognized that typical drumlin or drumlin ridges are
only the most emphatic of a variety of forms produced by the rub-
‘bing of ground-contact ice under thrust motion [see p. 429], and
that on the one hand these forms shade off into indefinite flutings or

ed

tKeilhack, K. Jahrbuch K. Preuss. geol. I.andesanstalt. 1896. p. 163-88,
2 Earth Sculpture. 1898. p. 234.

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Palmyra quadrangle. Drumlins on the Sodus-Newark meridian. The south edge
f the belt lies on the Phelps quadrangle.

onpEPaRTwENT UNIVERSITY OF THE STATE OF NEW YORK

IHN M. CLARKE

STATE GEOLOGIST

H.L.Fairchild 1905

BUELERIN it PEATE 5

af

STATE MUSEUM
DRUMLINS NORTHWEST OF PULASKI

Showing the varied directions. Only the more prominent forms are indicated.

T OF PULASKI QUADRANGLE

-¥ er eel ah aa? pe eae
EAD: "A5 eT SEE

apdieress eben alt vit

DRUMLINS OF CENTRAL WESTERN NEW YORK 395

moldirgs of the drift, and on the other hand are represented a

. scoured or rounded roche-moutonnéed rock hills (rocdrumlins), i

is probable that this class of phenomena will be found somewhat more

‘widely distributed in the glacial areas than has been supposed.

However. the requisite conditions for production of typical drum-
lins do not seem to have been commonly fulfilled, as vast areas -
of the glaciated territory seem never to have been subjected to the
drumlinizing movement of the ground-contact ice.

The land surface included in the great drumlin area of New York
is a belt about 35 miles-~ wide, bordering the south side of Lake
Ontario, and about 140 miles Jong (from Niagara river to Syracuse),
with a total area of about 5000 square miles. At least half of this
area, OF 2500 square miles, carries numerous and well developed
drumlins. The eastward extension of the drumlin area swings
around the east end of Lake Ontario as a belt 5 to 10 miles wide,
reaching past Watertown into the St Lawrence valley. An area in

Chautauqua county can not be estimated as the region is not topo-

graphically mapped, but the drumlins are scattering. |

The New York drumlin area probably includes not less than
10,000 drumlin crests, of which on a conservative estimate at least
6000 are indicated on the topographic sheets. Inthe districts where
the drumlins are close set from 20 to 35 can be counted in a square
of 4 square miles. Five drumlins to the square mile is common.
Three to the mile can not be more than the average, counting large —
and small, and on the 2500 square miles of well developed drumlin
topography this would give 7500 drumlins. Estimates have been
made by counting the separate drumlin summits or crests indicated
by the contour lines in certain limited districts and using the figures ©
for larger areas, with a result giving about 5000 crests for the 15

topographic sheets that cover the best parts of the drumlin area. On

the 216 square miles of the Palmyra quadrangle [pl. 4] the estimated
number of drumlin crests was 800, while an actual count gave 955.
Hundreds of minor ridges are beneath the recognition of the con-
tour lines.

The area of well developed drumlins extends eastward around the
east end of Lake Ontario, where they are specially interesting on
account of their attitude and peculiar form [pl. 5], and reaches
westward as far as the meridian of Batavia. The Pulaski, Sacketts
Harbor and Watertown sheets show the northeastward ending of

306 | NEW YORK STATE MUSEUM

the Ontario drumlin area, while the lower half of the Brockport,

Albion and Medina sheets show the westward termination as far as

the drumlin forms are indicated by the map contours [pl. 17]. West

of the Genesee river and near the Ontario shore distinct drumlins |

occur, shown in’plate 18, where the Iroquois waters were too deep
for effective erosion. Westward, on the Niagara-Genesee prairie,

the drumlin forms gradually become very elongated and indefinite —

low ridges, which slowly change to faint, invisible swells dying out

farther west. On the sheets toward Niagara the drumlinized . |
character of the surface is suggested only by the obliqueness of the

streams and contours to the general slope [pl. 19].
Southeastward the drumlin area terminates in peculiar fashion,

forming a decided point at Syracuse. The most easterly drumlins —

are the conspicuous group southeast of the city of Syracuse, which
stand on a base of Salina shales. The map shows no ‘well formed
drumlins north of Syracuse, over the Oneida lake depression, nor on
the high ground south of the Syracuse district. This extension of
strong drumlins as a tongue or point into a district otherwise
destitute of such forms is a striking and important fact.

East of Syracuse, as at Fayetteville, Canastota and Oneida, the
soft Salina shales which compose the irregular ground surface show
no effect of ice rubbing and carry only just enough drift to prove
the former presence of the ice sheet. The topography «is oa
mistaken for morainal, but is due to atmospheric erosion.

Plates 5 to 21 show some groups of drumlins, interesting for EY

either attitude or form, arranged somewhat in geographic order
from east to west. The Weedsport [pl. 11], Clyde and Palmyra
[pl. 4] sheets show the best display of drumlins, though other sheets
exhibit numerous and interesting forms.

In the zones of wave erosion by the glacial lakes the Pha
were cut or entirely removed. Lakes Warren and Dana were too
short-lived in the Ontario basin to do more -destructive work than
cutting notches in the drumlins and building the debris into
adjoining gravel spits and bars [pl. 17]. The same applies to Lake
Iroquois in its great Cayuga-Syracuse embayment, reaching from
Sodus to Richlarfd. But along the continuous or maturer shore
of Iroquois, extending from Niagara river to Sodus and from Rich-
land to Watertown, as well as along the living shore of Ontario, no
drumlin has been able to stand up alone against the waves;

|
|
|

fs

aRment UNIVERSITY OF THE STATE OF NEW YORK
ae STATE MUSEUM

BULLETIN 111 PLATE 6
RE AS cee,

on

“RIDGE DRUMLINS AND OVERLAPPING MORAINE

Moraine overlaps and replaces the drumlins on the north. Only the north border of the
rea is shaded.

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ARTMENT UNIVERSITY OF THE STATE OF NEW YORK
Eee acne STATE MUSEUM

BULLETIN 111 PLATE 7

2 Ni we vas 2
S = A
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FAIRHAVEN DRUMLEINS

a These broad ovals are nearer the dome-form than any. other group in New York.

DRUMLINS OF CENTRAL WESTERN NEW YORK 397

although they survived where immersed in more than 30 or 40 feet of
F Y yater. :
At Sodus Village the Iroquois beach, the “Ridge road,” is an
erosion cliff in several strong drumlins. Westward the north border
4 of the Syracuse-Rochester drumlin area swings to the south of the
beach and follows about west-southwest to the Genesee river, and
th ence west and north of west to the limits of the area northwest of
E atavia. The following places in order westward lie at the northern
= limit of abundant drumlins: Sodus, Williamson, Lincoln, Penfield,
i ‘Pittsford, Churchville, et eod Oak Orchard Swamp.

q Eastward from Sodus the Iroquois shore with less maturity curves
P southward around Sodus bay, but still marks a north limit of the
close set drumlins. The villages along this border are: South
| Sodus, Wayne Center, Rose, West Butler, the line passing 2 miles
| southeast of Wolcott. The northern border of ihe Syracuse-
| Rochester area curves so as to he approximately at right angles to
; the axial direction of the drumlins.

- South and east from Sodus bay, over the Montezuma and Oneida
owlands, the groups of drumlins stood as islands in the Iroquois

% "East and northeast from Sodus bay a somewhat distinct area of
heavy drumlins borders the shore of Ontario; and it ,is this series

assing lakeward from the Iroquois beach, into what had pees
p waters, a belt of drift forms, moraine or drumlins, gradually
pears which is abruptly terminated by the present Ontario beach.
would be interesting to know if the waters of Ontario hide drum-
is in their depths. As a series of heavy drumlins are opposing the
es all the way from Sodus to Oswego [pl. 7, 8], it seems quite cer-
that northern members of the group have escaped destruction
ubmersion in the deeper waters. |
e southern limits of the great drumlin area are even less
nite than the northern and can not be tersely stated. Approxi-
ely they may be given as follows: The western extremity of
area is bounded on the south by the shore of the ancient Lake
fea trom Indian Falls to Leroy. From Leroy the drumlins
re d south up the west slope of the Genesee valley to Mount

398 NEW YORK STATE MUSEUM

Morris, and extend westward on the high ground (1200 to 1800
feet) past Pavilion, Wyoming, Dale and Linden to Attica. East of
the Genesee river the southern limit may be taken asa line join- J
ing the south end of Conesus lake with the north ends of Hemlock @
and Honeoye lakes, the middle of Canandaigua lake and the north
ends of Seneca, Cayuga, Owasco and Skaneateles lakes; and thence —
eastward south of Syracuse to Fayetteville. The villages and cities ©

which nearly mark this boundary are Oakfield, Leroy, then the
southwestward stretch to Attica and Mount Morris, Conesus, Hem-
lock, Honeoye, Middlesex, Potter, Geneva, Waterloo, Seneca Falls,
Cayuga, Auburn, Skaneateles, Marcellus, Onondaga Hill, Jamesville —
and Fayetteville. :
In a broad way it may be said that the general area of drumlins —
covers all the low ground of the Ontario plain north of them
Finger lakes and reaches up the north-facing slope to high ground
approaching the divide. Between Honeoye and Canandaigua lakes ~
the drumlins lie as high as 1700 feet. e
Within the great drumlin area as described above some minor
divisions can be recognized With reference both to time and to
southern position the first series or group miay be designated as the —
Attica-Geneva series or the western Finger lakes series. This lies j
on the higher ground and includes the area between the Tonawanda
valley and Seneca lake, covering the section of the Genesee valley,
and Conesus and Canandaigua lakes as noted above.
The second series, Oakfield-Palmyra-Syracuse, lies on the low”
ground and includes the central part of the drumlin district and the
most striking drumlin topography, with a width in the central 7
part of about 20 miles. On the meridian of Rochester, east of the
Genesee river the first and second series are united.
A third and. still later series includes the drumlins which bor-

der Lake Ontario from Sodus eastward —the eastern Ontario
series. 3 :

The drumlinizing of the Niagara-Genesee prairie (subsequently the ©
Iroquois lake bottom) was probably contemporary with the second
and main series. The complete mapping of the somewhat indefinite

morainic belts, a study now in progress, will determine more certainly ©
the time relations of the several drumlin series. Plate 1 shows the
distribution as well as it can be portrayed at present.

A separate group of drumlins lies on the high ground bom

Lely i Lany YA \\ ly a gall 1s)
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WNW YORK

UNIVERSITY OF THE STATE OF NEW YORK

H.L Fairchild 1905

STATE MUSEUM

Ro
ia Pike) oye
J PAR i
Pht bhtall va De

fat ‘ i .
DISSECTION OF DRUMLINS BY ONTARIO WAVES

Min A
PART OF SODUS BAY QUADRANGLE.

se Spb a

-DRUMLINS OF CENTRAL WESTERN NEW YORK 399

autauqua lake, with direction pointing southeast [pl. ar].
nother group occurs about the north end of Cazenovia lake,
with altitude’ up to 1400 feet. Scattering drumlins occur in many
localities, and probably at even higher altitudes than noted above.

; The amount of Jand surface included in the principal drumlin

area is roughly estimated as 2500 square miles without including the
ortion east of Lake Ontario.

bs Some of the peculiarities of the main drumlin series, the Oakfield-
syracuse, in the matter of definite boundaries and minor grouping
should be noted here. These features, though difficult of verbal
description, appear very striking on a large map made by joining
| the topographic sheets. Along the northern border of this series
from Sodus east to Trondequoit depression the drumlins are quite
i abruptly replaced by morainic topography [pl. 15], the relationship
being discussed later [p. 424]. The north border of the eastern
b Ontario series Shows the change from drumlins to moraine even more
plainly [pl. 6].

On the southern borders the drumlin topography sometimes
| shades off into smooth drift [pl. 13], while in other districts it is
| lost in the bolder relief of the rock hills | pl.<16]. |
| e The most abrupt ending of the drumlin topography is along the
courses of ancient glacial river drainage. A series of drainage
iannels marks the definite southern limit-of the second drumlin

series from Victor to Geneva, and on the west of the Genesee at
‘oy and Mumford. A later drainage course, from Fairport to
yracuse, traverses the heart of the drumlin series, and seems
sponsible for the isolation of minor groups, the peculiar forms of
hich are indicated in plates 9 to 12.

i Orientation

The attitude of the drumlins with reference to compass direction
Mantes according to their position in. the area. The angular
Erections of their longer axes cover nearly a half circle. In the
istrict east of Lake Ontario they point east, that is they were
ped by a movement of the ice from the west. As we pass west-

w York to southwest; while on the Niagara-Genesee prairie,
the northwest part of the State, the direction is southwest

‘basin during the stage of waning which is represented by the 7

‘direction is strikingly confirmed by the study of the drumlins in

400 NEW YORK STATE MUSEUM

by west. This radial direction is shown on the general map,
plate 1, and the smaller maps, plates 5 to 17, show the attitude and
forms within the 20 foot contours. 4

The long axes of the drumlins indicate the direction of the latest.
vigorous movement of the ice sheet in their locality, and the —
variant directions of the drumlins throughout the whole area prove

a radial or spreading flow of the ice mass that rested in the Ontario ©

drumlin formation. ; |
This consonance of the drumlin attitude-to the latest ice flow

outlying districts. The Chautauqua drumlins point southeast, in
harmony with the spreading flow of the Erian lobe of the wan- j
ing ice sheet. On the other hand, the drumlins of the Water-
town district, east of Lake Ontario, point southwest, conform-
ing to the latest flow of the thinning ice in the StLawrence
valley.

Another interesting fact to be noted in this connection is that
the axial direction is not always uniform along the same meridian.
If the topographic control over the ice movement changed with the
varying latitude of the ice front, as the latter was receding, the |
drumlins record that fact. For example, 20 miles south of Roches- ©
ter the ice margin was guided by the Conesus, Hemlock and
Honeoye valleys and the drumlins are north and south. But on the ~
same meridian, only 6 to 12 miles south of Rochester, the drumlins ©
point to the southwest, the ice margin being controlled by the
Genesee valley and the thrust being from the northeast. : '

The radial or spreading flow of the ice at any single stage must bel
found by a comparison of the drumlin directions within a single
series of drumlins, that is, drumlins which were formed simul-
taneously. If we take the second, or .Oakfield-Syracuse, series we
find the axial directions point as follows: At Oakfield, s.55° to’
60° w.; Fairport to Palmyra south; Syracuse, s. 30° e. Taking the
ae or eastern Ontario, series, the drumlins are north and south at
Sodus bay; at Oswego, s. 30° e.; Mexico, southeast ; Pulaski,
e. 20° s.; Sandy Creek, east. |

A peculiar confirmation of the genetic relation between drum-
lin attitude and ice-flow direction is found-in the Pulaski region. _
Passing northeastward around the corner of Lake Ontario (Mexico.

CATONDEPARTMEWT UNIVERSITY OF THE STATE OF NEW YORK

H . CLARKE

STATE MUSEUM BULLETIN 111 PLATE 9
; \ ee, | i,

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ART OF BALDWINSVILLE QUADRANGLE. : H.L.Fa

DRUMLINS GROUPED IN ISLAND MASSES

ye

ZN IN

So —— <4)
if Ul

mi

irchild 1905

_-—s* The valleys are carved in Salina shale, which forms at least the base of the drumlins up
__ to 500 feet or higher.

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Mts cosernae H.L.Fairchild 19(
te _ The drumlin-shaped forms in the upper part of the map are Salina (Vernon) shale.

..
es.
peed

Ry.

DRUMLINS OF CENTRAL WESTERN NEW YORK 4OI

we find, as noted above, that the direction toward which the
imlins point veers from southeast to east. But as we pass on
-h some 10 miles, to Ellisburg and Belleville, we find the drum-
s pointing southwest, or in direction nearly opposed to the drum-
between Oswego and Mexico, |

These opposing directions represent ice-flow movement at dif-
1t stages of the waning ice body. While the Ontarian mass
t covered the Oswego-Pulaski district the radial flow produced
forms which point southeast at Oswego and east at Sandy
ek. But during the latest stage of the ice in the basin the
w of the St Lawrence valley lobe produced the southwest-pointing
as between Ellisburg and Watertown.

will now be recognized that if the southeast-pointing forms
re raade by an earlier flow of the same waning ice mass that pro- —
ced the later southwest-directed forms then somewhere between
two opposing forms the drumlinized drift should indicate a
ing, swinging or pivotal motion of the ice. As a matter of

ast. As seen from the north or south the characteristic profile
usually clear, but with change in point of view, looking from

a of these contrawise forms should have received expression
she topographic sheets.

From whatever direction we view many of these hills the drumlin
m appears. In many cases one detects a faint but distinct mold-

s of the drift in direction highly inclined to the main form.

metimes an irregular surface which is regarded as morainal

. ee iiinere are a of SE ae surface and

Fie peculiar forms of the Pulaski drumlins were made Hee the facts recorded as side notes

making special study of other phenomena, and their significance was not appreciated at

402 NEW YORK STATE MUSEUM

in some areas, as north and west of Pulaski, the moraine character
prevails. Frequently a drumlin form as viewed from some distance
becomes irregular and morainal in minor relief on nearer view.
Sometimes the moraine surface is equally puzzling ; smooth ridging
or ribbing making one doubtful whether to map the area as moraine
or drumlinized drift. Such areas occur southwest of Pulaski [pl. s]
and northwest of Sandy Creek. 7
_ One important point which has a bearing on the origin of drum-
lins should be noted here. The secondary or contrawise forms §
do not seem to have been made by the cutting or carving of the
primary forms but to have been produced by the addition or plaster-
ing on of the later form. The work seems to have been con-
structional, not erosional. | a

The explanation of these exceptional features would seem to be-
that the main and larger drumlin forms were made by the eastward
motion of the ice; and that the minor molding, at a high angle and
usually southward, was produced when the waning ice in this
district felt directly the thrust from the St Lawrence valley. It)
does not appear that the molding of the drift is pronounced in
directions intermediate between eastward and southward. Possibly
while the ice flow was changing from eastward to southward it was
not relatively so vigorous, but 1t is more probable that only the latest
of the minor ridging is conspicuously preserved. |

Relation to larger topography

A glance at plate 1 shows that the general drumlin area covers ©
ground of all altitudes from the level of Lake Ontario (and they
probably occur in the depths of Ontario) up to about 1700 feet;
this highest edge of the drumlin belt lying west of Canan-—
daigua lake [pl 16]. West of the Seneca valley they usually reach ©
up to high ground, 1100 to 1500 feet. In the low north and south
depression of the Seneca and Cayuga valleys, where we might
expect them to be well developed, they are weak or wanting above
500 or 600 feet [pl. 3, fig 2]. While scattering drumlins may occur
im poor form between the eastern members of the Finger lakes it
may be emphatically stated that the area of close set and well
developed drumlins does not reach south on the high ground east
of Seneca lake, but that extensions of the drumlin area do reach up

on the high ground west of Seneca lake and as far west as to the

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" epucaTionperarTmenr UNIVERSITY OF THE STATE OF NEW YORK.
JOHN M.CLARKE :
_ STATE GEOLOGIST STATE MUSEUM

BULLETIN 111 PLATE 11

|

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Fell

.L.Fairchild 1905

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Hicrsirchild 1905

DRUMLIN MASS IN MONTEZUMA MARSHES

BULLETIN 111 PLATE 12

4 { Ei

3
44

STATE MUSEUM

The ‘‘heart’’ of the drumlin area.

2 artuent UNIVERSITY OF THE STATE OF NEW YORK

ida),

AMURELY

Wi

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Bae ald

a

DRUMLINS OF CENTRAL WESTERN NEW YORK 403

_ Tonawanda valley. This distribution of the drumlins indicates that
altitude and grosser topography are not alone controlling factors in
_ the drumlin formation. .

q The most massive development of -the drumlins is on the. low
“ ground north of the Finger lakes, and chiefly under 500 feet altitude.

This great development of the drumlins on the low Ontario plain and

their comparative absence on the higher ground facing the ice
sheet is most striking in the central and eastern part of the drumlin

bs belt. -

It is important to note that the district of highland drumlins, the
_ western extension of the drumlin area, is where the later ice move-
- ment and the drumlin direction coincide with the general direction

; q of the main ice movement, that is, toward the southwest; while the

_ district of no elevated drumlins, east of Seneca valley, is where the
3 drumlin diréction 1s oblique or nearly at right angles to the direction
of flow of the thicker ice.

_ The production or nonproduction of drumlins is believed to
depend in part on the abundance and character of the bottom
drift of the ice sheet, but chiefly on the active movement of the

. = bottom ice, due to thrust from the rear. The absence of strong

_ drumlins on the gently ascending slopes between Seneca and

_ Owasco lakes may be partly due to the capacious preglacial val-
leys in the area north of the Finger lakes, which served as catch-
ment for the lower drift. The absence of any large amount of
drift, in the form of either drumlins or moraines, in the belt of
_ open valleys [pl. 2] suggests that the last 1ce which lay on this
_ territory was comparatively clear of drift. It would seem that the
greater burden of drift had been either rafted over the level of the
_ open valleys to the higher valley heads moraine farther south, or
was held in the lowest ice, and built into the drumlins farther
north. |

As stated above [p. 369| the land surface east of Syracuse never
felt Bere rubbing aetion ef the ice, sheet The Syracuse’ distrret
was subjected to the thrust of a tongue of ice pushed southeast-
ward from the spreading Ontarian mass. The southeastward and
southward flow was not sufficient to reach the land surface over the
_ Oneida lake region nor over the high ground east of Seneca valley.

.% However, the land surface west of the Seneca valley, lying where the

latest ice movement was the same as the principal ice movement,

404 NEW YORK STATE MUSEUM

toward the southwest, felt the molding effect of the ice thrust dur-

ing the waning stage.

Relation to underlying rock strata

A glance at any stratigraphic map of New York State will show
that the dominant drumlin area, north of the Finger lakes, lies on
the low ground north of the outcrop of limestones formerly called
Helderberg and Corniferous and over the belt of strata now known
as Cayugan (Salina), Niagaran and Oswegan (Medina), naming them
in descending stratigraphic order, or from south to north. These
strata are chiefly shales, with relatively thin limestones in the
Niagaran and some sandstone beds in the Oswegan. |

The following table gives the approximate thickness of the several
strata along the Cayuga meridian (corrections supplied by Mr C, A,
Hartnagel of the State Geological Survey).

New York rocks along the Cayuga meridian

Thickness
Divisions in feet Kind of rock
ea Hamilton I 140 Shale
a Marcellus pas one Shale
Ulsterian Onondaga 80. Limestone
Oriskanian Oriskany 3 Sandstone
Manlius 26 Limestone
. Rondout Limestone
Cayugan ; :
Cobleskill 6 Limestone
Salina I 400 Shale
( Lockport 5 Limestone
Niagaran { Rochester Shale
| Clinton 7 80 Shale and limestone
§ Medina | 950 Shale and sandstone
Oswegan
Oswego 200 Sandstone
Canoe Loraine ue Shale sd
Utes Shale

The drift supply for the drumlins of any district was derived
mainly from the strata immediately northward. The above table
shows that rocks beneath the limestones which inclose the Oriskany
are mainly shales of great thickness. Counting the Medina
as one fourth sandstone and the Niagaran as half limestone we
have 3130 feet of shale, 200 feet of limestone and 44o feet of

CATIONDEPARTwENT UNIVERSITY OF THE STATE OF NEW YORK
OHN M. CLARKE
ATE a STATE MUSE UM BULLETIN 111 PLATE 13
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Derr Moew OF THE MAIN DRUMLIN dgueacms

The terminal mor aine lies in front of the attenuated drumlin border

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' DRUMLINS OF THE MORMON HILL GROUP

_ The south termination is abrupt against a glacial river channel.

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DRUMLINS OF CENTRAL WESTERN NEW YORK 405

isa dstone. All these strata have a decided southward dip which
gave outcrops projecting northward against the ice advance. By
long eras of preglacial weathering these exposures of shale and lhme-
tone afforded a large supply of plastic drift tothe bottom ice. It is
ieved that the rock rubbish was not in any stage of the ice work
ried far away, but on the contrary was plastered into the drum-
in masses. The thick clay strata supplied a burden of unusually
cl oy and adhesive drift ; and it seems probable that the adhesive
and 1 plastic character of ae lower drift was a contributory factor in
the upbuilding of the drumlins, specially the taller ones.

| Form and dimensions

_ These elements are very variable. The ordinary shape of the
pes in western New York is an elongated oval, the length being
hree to five times the breadth. Occasionally they are short ovals, |
a faa rarely approach the mammillary form, but much more frequently
they are long or attenuated ridges. The elongated or ridge form is
th characteristic New York type, though other forms occur
rf: eeauently, except the dome. .

_ Considering horizontal dimensions the several bees may be
Be tingiished as the mammilla or dome; the oval; the slender
oval or short ridge; and the linear or attenuated ridge. The two
latter forms include the great majority of New York drumlins. It
is an important fact that the several types are not intermingled
are. separately grouped, certain districts exhibiting some ope
ticular iype almost exclusively. This is fairly illustrated; i
selection from the topographic sheets ; the oval form, large ot
“sr mall, being shown in plates 7 and 11, a Fairhaven, Syracuse and
“Weedsport districts ; plates 12 and 14 showing the short ridges in
‘the ‘Clyde- -Palmyra ace: while the long ridges are shown in
plates 6 and 19, the se district and the Niagara-Genesee
prairie. The very slender, linear ridges are.often too low or weak to
be shown by 20 foot contours, but an example which appears on the
1 P is here given as plate 13, the eee) north of Waterloo and
Seneca Falls.

Ee The lengthwise profile of the shorter sen Gis is an Sean curve,
nvex to the sky, and characteristically more abrupt or steeper at
- north end, The crest line of the longer ridges is commonly |
st a straight line, which appears to the eye as true as if
to a “ straightedge” [pl. 30]. The south ends of all drumlins,

406 NEW YORK STATE MUSEUM

except the steeper ovals and domes, taper off into the general sheet
of till unless eroded by waves or other agency. —

In cross-section the variation of profile is more limited than in —
longitudinal section. The summits naturally have a symmetric

curve. Unsymmetric but yet convex summits may be produced by

the drumlin process, but sharp crests, as in plates 29, 34 and 36 are q
regarded as an effect of later erosion. In some cases the erosion of 3

the sides of the drumlin has gone so far as to gnaw into the summit

and produce a scalioped or wavy or broken crest line. Asarulethe —
shorter drumlins have the flatter cross-section profile, while the
long and the linear ridges may have either a crest curve of short 4
radius with steep side slopes or a broad summit and semicircular —

cross profile.

The junction of the convex drumlin with the horizontal ground —
surface naturally gives a concave slope at the drumlin base.. Above
this concave basal slope all drumlin surfaces are regarded as
normally convex, and departures from convexity are due to some ,
interference with the constructive process or to some subsequent

effect. Two or more drumlins may overlap, or blend, or even be
superposed [see p. 409] so as to produce irregular or unusual forms.
Morainal drift is frequently banked against the sides and bases of
the drumlins so as to change the true form. Erosion by the waters
of glacial outflow may have cut the slopes and even the crests of
drumlins, but decided crest cutting has been infrequently seen in
New York, though conspicuous in Massachusetts.? 3
Vertical ridging or ribbing of the side of the drumlin is thought to
be positively erosional, either by glacial waters or by postglacial

storm wash and weathering. On the other hand longitudinal flut- 4

ing or molding is regarded as a constructional effect of the drumlin-

making progress, |
‘With very few exceptions the drumlins are cleared of timber and

their surfaces are under cultivation, as they afford the best soils.

Some of the minor irregularities of surface may be subdued by —

the farm cultivation, but when the elements contributing to their
erosion are considered it is remarkable that they are so well
preserved. In the great majority of cases they seem to pre-
serve their original form with practically their natural surfaces.

1 Barton, George H. Glacial Origin of Channels on Drumlins. Geol. Soc. Am. Bul. 6: —

8-13.

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EDUCATIONDEPaRTMENT UNIVERSITY OF THE STATE OF NEW YORK
Meee amotocise STATE MUSEUM BHOLETN ta PLATE 4S
(ee em (Z

WALWORTH DRUMLINS

Moraine drift is scattered among the drumlins, wholly replacing them onthe north. The
Iroquois beach (‘‘ Ridge road’’)forms, by erosion, the north limit of the moraine.

Cb: bt si
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A ilk ci

DRUMLINS OF CENTRAL WESTERN NEW YORK 407
e

The type of form least exemplified in New York is the dome-
shaped. While such may rarely be found they certainly do not

characterize any district. The group of drumlins which most nearly

approaches the mammillary form, judging from the topographic
sheets, lies in the neighborhood of Fairhaven bay, and is partly shown
in plate 7. The oval form is excellently shown on the Weedsport
sheet [pl. rz]. The long oval or short ridge, the “dolphin back ”
shape, probably includes a majority of all the New York drumlins,
and is the most widely distributed. A massive development may be
seen on the Palmyra sheet, plate 4. Probably this form should
be regarded as the typical drumlin form, from which the dome

on the one hand and the linear ridge on the other are extreme

variations. : 2
The long drumlin ridges, which are specially pronounced in New

‘York and are therefore regarded as the New York type, are well

displayed on the Clyde, Auburn, Oswego and Brockport sheets.
There are two extreme varieties of the ridge form, the large and the
small. The large form includes broad, low swells or rolls which if
lying alone or far separated may not be recognized as of drumlin

mature. They are not often indicated by the map contouring.

These low, broad moldings of the till are the common and only
form over most of the surface of the Niagara-Genesee prairie.
Passing west on the Rome, Watertown and Ogdensburg Railroad,

the change can be readily seen from quite typical long drumlins

near the Genesee river [pl. 18] to very long swells of low relief,
which if not at all indicated by the 20 foot contours may be
recognized by the shallow cuts for the railroad grade. Westward

these rolls gradually fade into gentle’ undulations of the surface,

quite imperceptible except by the up and down grades of the rail-
Eeaee aree areas are perfectly flat to the eye. Buildings are
visible for miles in different directions on the plain unless hidden by
trees. The roads stretch great distances, ending to view only
by the overarching shade trees or by a turn in direction. That

this smooth country has been ice-molded is shown by the stream

flow, which is northeast or decidedly oblique to the general slope.
The low relief and the oblique stream control is well shown in
plate ro. | |

These southwest-pointing drumlin ridges occur in strong develop-
ment southwest of Alden and west and southwest of Buffalo over

408 _ “NEW YORK STATE MUSEUM

he lower and smoother plain. The contouring on the Erie count a a
sheets, the Attica, Depew, Buffalo, and other quadrangles to the ©
south, fails to properly indicate the drumlinizing of the land 4
surface. As the ridges liein the smooth country occupied by the 4
glacial Lake Warren and the subsequent falling waters, and as they a
have the southwest direction parallel with the generai contours and

the lake shore lines, some of the smaller ridges are liable to be mis-
taken, in distant view, for huge wave-built bars or beaches.

The small variety of the long ridges is displayed in the Lyons-
Clyde-Savannah district, where the primary drumlins include —
between them a secondary or minor order of ridges. These inferior —
ridges are straight, parallel, side by side, and often not larger than 4
large railway embankments. They are not good subjects for pho- ©
tography but plates 32 and 33 are examples. These attenuated,
intermediate ridges prove the molding action of the ice, and —
its drumlin-making tendency, even in the hollows between the ~
larger structures. The major and minor ridges taken together —
suggest comparison with a piece of wood molding “ struck ‘i by the @
planing machine. This comparison is even better if we take the —
drumlins which exhibit longitudinal ribbing or fluting along their 7

sides or bases. This longitudinal molding on the slopes of drum- —
lins-is certainly constructional and not due to any subsequent or |
erosional effect, as are the vertical forms."

To the observant traveler on the railroads between Rochester and
Syracuse the statement that the longitudinal drumlin profile is j
always convex seems untrue, because decided concave notching may —
be seen on both north and south ends of the drumliins. These are F
due to subsequent wave erosion by glacial lake waters. Some work
of this kind was done at higher levels by the Warren and Dana ‘
waters [pl. 17], but the most conspicuous notching is in the area of —
the Iroquois waters. The pronounced erosive work illustrated on 3
the shore of the living Ontario [pl. 7, 8] and along the “ Ridge
road” or ancient shore of the extinct Iroquuvis [pl. 4] may be seen —
in less degree but yet clearly between Lyons and Syracuse from the —
trains of the New York Central and the West Shore Railroads. §
Plates 36, 37 and 39 are views taken from the railroads. a

= ——

x Speaking of these ridges D. F. Lincoln has said: “‘ From this they grade downward to little
ridgelike elevations of 5 feet in hight and a furlong in length. Even these are quite distinct to |

the eye, rising from the uniformly level plain.”

_—--» ~eurvrun, are Crowded

EDUCATION DEPARTMENT UNIVER: THE
JOHN M. CLARKE ‘SITY OF STATE OF NEW YORK
STATE MUSEUM

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HIGH-LEVEL DRUMLINS BANKED AGAINST THE

BRISTOL HILLS

‘The great Bristol hills are hard rocks and quite unaffected by the glacier. The drumlins
southwest of Bristol Center are probably the highest above sea In western New York.

" HiL-Fairchild 1905

e

a

DRUMLINS OF CENTRAL WESTERN NEW YORK 409

f _ islands in the Iroquois waters seems capricious. Some drumlins

_ This wave cutting of the drumlins which held their heads up as
- which from their location must have been exposed to severe wave

a impact from the direction of the heaviest winds (mainly northwest)
i exhibited little effect, while others [pl. 38] which had more sheltered
ee

_ positions or were exposed only to southerly winds are decidedly cut.
The amount of wave cutting seems to have depended in no small
fe degree on the composition and texture of the till.
One singular effect of the end erosion of the isolated drumlins is
: to give a bent appearance to the cut end. Oblique erosion of. the
| originally rounded end causes the crest line of the ridge to bend
Seaway abruptly, to the leeward, from the axial line of the hill. In
some cases this change in the direction of the crest line Is the best
evidence of erosion, for it is believed that the original crest of the
stoss” or struck end of the drumlin must have been true to the
» axial line. Examples of these twisted-nose drumlins are rather
3 poorly shown in plates 36 and 37.

A singular form of drumlin is found in the district south and
southwest of Rochester, illustrated in plates 4o to 42. This sug-
2 gests one drumlin superposed on another; a sort of two-story
| drumlin. They were first noted in connection with the search for

evidences of Dana waters. Some of the concave slopes coincide
with the Dana level and possibly the. features have been rarely
accentuated by wave erosion, but the form is found at other levels.
Moreover, iieeestmaces, Of the two-story drumlins have the
characters of ice molding, the lines are out of horizontality, and
Grostonal characters wanting. The form is believed to be the
product of the ice work, and perhaps due to two stages of the con-
structional process, or to a slight change in the direction of the ice
movement.

These double-deck drumlins have been found only in the district
at the north end of the larger Genesee valley, and on either side
i@eeot the valley. It is suggested that the variation or change in the
_ upbuilding process which caused this peculiarity in form may have
| ; been related to a change in the direction of ice flow due to the
| influence of the Genesee valley on the thinning ice sheet. ,

t The cross profile of a drumlin is naturally subequal or symmetrical,
| but there is modification of the slopes when two or more drumlins
lying close together, either side by side or in echelon, are crowded

aA

410 NEW YORK STATE MUSEUM

in their growth or even blended. Asymmetry may be due to some

local variation in the ice movement, apart from the crowding in

construction.

Sometimes the drumlins have an outline when seen endwise that”

resembles the normal longitudinal profile. This abnormal form has

been seen frequently in Wayne county west and northwest of Wal- —

worth [pl. 15]. This form is not due to change of ice flow direction
(which accounts for the similar appearances in the Pulaski district)

but to irregular construction, and perhaps to ultimate union of 4

primarily distinct drumlins. In the dominant drumlin area the grow-
ing drumlins seem to have frequently fused together so as to give
unbalanced cross-section profiles, but such drumlin masses have in
longitudinal outline the characteristic curve.

Dimensions. The size and dimensions of drumlins are variable,

within limits, according to the quantity and quality of the drift and

the depth and impulse of the ice sheet. The smaller or infantile
drumlins do not usually have good or characteristic forms unless
they are of the slender type or small, attenuated ridges, which may
be small in cross-section and yet retain a distinctive character as
ice-molded till. 3 |

There seems to be a limit to the hight of individual drumlins, this
being in New York about 200 feet. Using the map contours for
determining the base of the drumlin as well as the summit altitude
(an inexact basis, with maximum error of 40 feet) only one drumlin
is found with altitude over 200 feet. At some point the upbuilding
process is antagonized. by the eroding or leveling tendency and a
balance is struck between the opposing forces which limits extreme
hight, and results, apparently, in the production of multiple ridges
of moderate size instead of one huge ridge. This principle seems
to be illustrated in the orm of the peculiar groups in the Syracuse
region, described later !p. 429 and pl. 9].

The most conspicuous drumlins, striking because of their isolation,
like those rising out of.the Montezuma marshes, are not the highest.
Using the map contours, as noted above, for approximate data along
with the figures frequently given on the map for definite altitudes
of many higher drumlins, the following table has been compiled.

This gives the approximate altitudes of base and summit and the

individual hight of a considerable number of New-York drumlins
in different districts,

STATE MUSEUM

UNIVERSITY oF THE STATE OF NEW YORK

UCATION DEPARTMENT
OHN M. CLARKE

p24)
J

STATE GEOLOGIST

BULLETIN 111 PLATE 17

H.L- Fairchild 1905

ELBA DRUMLINS
The northern drumlins bear the gravel spits and wave-cut cliffs of Lake Dana, at about
700 feet. At about 880 feet, on the south edge of the map, is the shore of Lake Warren.

PART OF ALBION QUADRANGLE.

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160 .

DRUMLINS OF CENTRAL WESTERN NEW YORK 411
Altitude and hight of highest drumlins
Base and summit
Designation altitudes Hight
P Meridian of Rochester
Seeeeeitrder hill. 2m.n.w. of West Rush ........,....0.. ieee’! O2O=860 180
> Huckleberry hill, 2 m. w. of Lima.......... Sees goo-1054 154
" 3 Reamiam nvlly2m. ne. of Livonia............0..0. ee eee 1040-1194 154
ie Penn im usw. Of Livonia. :......08 setae! oetaroinens 920 -1080 160
iP Meridian of Palmyra and Macedon
3 Pennie om. m.w. of Maridm . ..a.....0-cesectees 480-665 185
| bs Triangulation station, 4 m. s.w. of Canandaigua....... 1040-1201
to ? hill, 1m. n. of Palmyra............ 480 633 150
‘ 7 lee Zane nie. Ole Palmyra: tLe Ys desc noes 500-670 170
Setonmon mill 4 m.s. of Palmyra... ........-. Ww oaack tel ce 600-700 100
Meridian of Sodus-Newark
Siriameulation station, 4 m. w. of Sodus .......... F 440-595 TS
imameulation station, Im. s.w. of Sodus..........0... 460-620 160
; Pee mete S eit S. Of SOUS 3... ee ee en vee eee tee 440-640 200
: eC MMONmLes. Of SOMUS: 657. i4 sod oaslaescccssw cece se’ 460-680 220
raneulation station, 2m. s. of Clifton Springs.......- 700-860 160
Meridian of Sodus bay-Clyde
Bimammoysnhuit 2m. ¢..of Sodus bay: ......0....+eeerees 250-400 150
* ? mM erlanMbetin yy: TOL: NOSE Si. Soc ek. be wae woes 420-600 180
Mimiame ulation station, 2% m.s. of Clyde......... Bea ese 420-600 | 180
Meridian of Fairhaven
? uleeoanieennen Of Fairhaven. 2. 2... 6. <4 le eco eas 250-400 150
meee. see. of Montezuma........... ee ees 1520 700 180
Meridian of Oswego-Weedsport-Auburn eA
Maaneniation station, 4m. n.w. of Cato ....c..cc.c00es 400-567 167
? lomeSMTIN NTI. (Olin. CAL Ore les ccth arate b Geer ois, ee arens 440-620 180
? uterine Ww. OF Caton oo. ss wes Me aps rclbes Sexe - 420-600 180
? flileerttetin ae OL Wieedsporto.. <e las ae 5 occ 440-620 180 -
Z iiniancwlatvon station, 2m.s. of Weedsport ......:.... 600-740 140
Meridian of Fulton-Jordan-Skaneateles
PeA miss. Of Jordan... ... 04. ee ce eae ess c eee 660-800 140
Peer ceniie seme mew. Of Skaneateles .. ..0c.sccces vecnes 880-996 116
Region of Syracuse
? Emilemcmnneatows Of Camilluse.,.s2 sc cis eis es oes eee 700-860 160
? Meese nor Camillus om. vc see es dalsde oe es 640-760 120
Pitamanlatton station, 3 m. e. of Camillus.............. 660-799 140
Pramewlation station, 3 m.e. of Camillus........5...... 580-736 156
? iitiesemassje* Of Syracuse... o2u2. «ks 660-805 145

_1It isasingular coincidence that the celebrated drumlin, the ‘‘ Mormon hill” [pl. 29, 30},
in which Joseph Smith claimed to have found the golden plates of the Book of Mormon, should
have as its altitude the centennial multiple of the sacred number seven, in English feet. The
hight of the hill was not known until the recent topographic survey, but the Latter Day Saints
May claim that their prophet had inspired knowledge or divine guidance,

412 NEW YORK STATE MUSEUM

It will be noted that only two. drumlins in the above table lift
their summits 200 feet above their platform, though several approach |
that hight. :

The length of the drumlins is quite as variable as their hight, but
it can not be well determined from the map contours, as a relief of —
less than 20 feet may carry a distinct ridge for a long distance, ~
The long ridges of drumlinized drift which specially characterize —
the drift surface in the northwest corner of the State, including the —
Niagara-Genesee prairie, are almost unrecognized by the topographic |
map. — ;

Scores of drumlins can be found on the map with a contoured —
length of a mile, or even a mile and a quarter. A length of 1% ~
miles is not rare, but 2 miles is extreme. Perhaps the longest well —
contoured forms are in the Oswego district, shown in plate 6. |

The very long drumlins are sometimes produced by the close —
welding of overlapping ridges. en :

Composition and structure

The material composing the New York drumlins is very compact _
till. The writer recollects only one or two instances in which water-
laid drift has been found unequivocally incorporated in the drumlin 3
mass. Gravel and sand are frequently found on the flanks of the
drumlins, specially where they were exposed to wave work of the
glacial lakes, but the experienced observer could never mistake this
for drumlin material. Water-laid drift may be expected on the ©
surface of the drumlins as an occasional product of superficial
stream work at or near the ice border. In morainal areas the

marginal drift, kame or till, may be scattered on and among the
drumlins, and sometimes in such abundance as to obscure Or. per-
haps partially bury the drumlin forms. Such a case is found in the. @
Junius kame moraine, midway between Geneva and Lyons. How-
ever, this superficial morainal drift must not be mistaken for nor
confused with the drumlin material, as it is not only emphatically
distinct in its genesis from the subglacial drumlin mass but sub-
sequent in time of deposition. :

Only two instances have been found by the writer of water-laid
drift distinctly within the drumlin mass. In the northeast edge of
the village of Lyons, on Phelps st., a small drumlinlike ridge of till
about 500 feet long and 150 feet wide, lying on the east flank of a

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413

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BULLETIN 111 PLATE 18

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DRUMLINS OF CENTRAL WESTERN NEW YORK 413

_ larger drumlin ridge, has 15 feet depth of till over a base of sand 7
but the sand substratum is restricted to the small ridge.

In a recent extensive examination of the internal structure of
drumlins, to be described below, a bed of sand was found in the
interior mass of a drumlin, situated 2 miles northeast of Fairhaven
bay and south of Juniper pond. The waves of Lake Ontario have
dissected the drumlin obliquely, exposing a section of till about 100
feet high. About midway in the hight of the cliff is an irregular

layer of sand, 2 to 3 feet thick and of considerable but indefinite

extent. The sand shows no clear bedding and seems to have been ~
crushed and worked over by the ice rubbing. The extreme rarity of
such inclusions of water-laid drift in the drumlins of New. York is a

_ conclusive argument against the theory that they are erosional

forms, produced by overriding and reshaping of terminal moraines.

F This point will be discussed later.

The drumlin till, specially in the deeper layers, is decidedly more
compact and harder than the ordinary sheet till, and the included

_ stones of all sizes are more generally abraded. ‘The material gives

evidence of movement under pressure ; it is emphatically the glacial

grist.
The proportion of crystalline and far-brought material is appar-

| ently less than in terminal moraine deposits, but examination has

not been sufficiently thorough to indicate percentages. In any belt

it will probably be found that the proportion of material derived

from the subjacent strata or the rocks immediately northward is
fareger in the drumlins than in the moraines. In other words,

, drumlins represent, at least in central New York, the subglacial or
“ground moraine” drift.

Rocdrumlins. Between Palmyra and Syracuse the foundation of
the drumlins is Salina shale, mostly the soft red and green beds

_ called Vernon shales. All the deeper valleys are cut in this shale,

which may be seen on the slopes as bare patches of bright colors, —

: Bea@eand light green. An excellent exposure may be seen at the
~ “blue cut” on the south side of the West Shore and the New York
_ Central Railroads midway between Newark and Lyons; and at the

time of this writing (September 1905) the electric road building

min that district is making many exposures. . At the “blue cut”
_ the Vernon reaches 60 feet above the railroad, or to the hight of
_ about 480 feet, judging from the map contours. In the region of

414 NEW YORK STATE MUSEUM

Jordan and Memphis these’shales forming the walls and bottom
of the broad valley are eroded into forms simulating morainal
topography. (This resemblance of the shale erosion forms to
moraines is very pronounced all the way east to Oneida, and even
the experienced geologist who is new to the region will make wrong
diagnosis if he decides by the forms as seen from a distance.)

In the Jordan-Memphis district the Vernon shales reach up:

over 500 feet, while the lake and stream fillings in the valleys are
about 4oo feet altitude. The Vernon shales, therefore, extend
upward about 100 feet above the lowlands and are overlain by the
somewhat harder but yet soft gypsum-bearing Camillus shales.
East of Jordan they form the common platform from which the
drumlins rise [pl. 9, ro]. But west of Jordan, as far at least as

‘Newark, the drumlins are situated much lower, their bases being
contoured [pl. 11, 12] by the 4oo or 420 foot contour, and many rising

out of the Montezuma marshes as if partly buried under lake
deposits. It appears, therefore, that in the Weedsport-Lyons belt
the Vernon and Camillus shales belong in the same horizontal plane
or topographic horizon as the drumlins, and the interesting and
important question arises if the drumlin forms may not be partly
shale instead of till. Some study of this problem has been made
with definite results. ‘The drumlins show only till at the surface, in
nearly all cases. Often this may be only a veneer or varnish of
drift rubbed into the soft shale.. The West Shore” Ranroqdenar
several good cuttings through drumlins in the stretch west of Port
Byron which ought to reveal interior composition and structure, but
the cut slopes are so coated with wash from the upper material that
to casual inspection they appear as till.

One and one half miles northeast of Port Byron the red Vernon
shales appear clearly on the slopes and at the summit of a drumlin-
shaped hill having a summit contour of 460 feet, = ighis aii
indicated in the lower left hand corner of plate 11. Here we cer-
tainly have a drumlin form in rock, a rocdrumlin. It is very likely
that other of the lower drumlin forms may be chiefly shale with
only a veneer of drift, and it is more than likely that some of the
larger drumlins have a base or core of shale.

All the western central New York rocks have a decided southerly

dip. It is evident, therefore, that north of the Syracwseayomes

parallel the strata should lie at increasingly higher elevation.

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TT QUADRANGLE.

DRUMLINIZED SURFACE H.L.Fairchild 1905

Near the west end of the Niagara-Genesee prairie. Compare plate 18. The ice-molding
earries the streams oblique to the slope. Surface smoothed by Iroquois waters.

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AHN M. CLARKE ‘
STATE GEOLOGIST BULLETIN 111 PLATE 20

The attitude of the drumlins shows how the later ice flow in the Genesee valley was
diverted from the general southwest direction. Not all the drumlins are indicated.

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>. DRUMLINS OF CENTRAL WESTERN NEW YORK AI5

aa

The vertical or stratigraphical range of the Vernon shales, which
are several hundred feet in thickness (the thickness of the whole

aqpeegey

eee

group of Salina shales is about 1400 feet, see page 404) would include

_ territory. An examination was made of the hills west of Baldwins-
ville with a result not unexpected. It was found that all the drumlin

eae

_ forms are clearly composed of red shale, with only an apology of till
IK covering. All the hills in the upper half of the map, plate 10, and
| lying between the two north-leading valleys. are known to be not
| drumlins but rocdrumlins.

“At first sight these hills would be regarded without question as
true drumlins, but there are decided though refined differences
_which appear on closer study. The rocdrumlins are not so sym-
| _ metrical as the till forms; the slopes are less regular; and the struck
: _ ends are liable to be more abrupt and irregular and with less con-
: vexity. The differences are clear when once recognized, and are
| : fundamental. The 20 foot contours of the map even reveal a differ-
| ence. Looking at plate ro it will be noted that the bases of the hills
| "are indefinite, and that as hills they do not possess the strong indi- .
| yiduality of the drumlins, as shown in plates rr and 16, for example.
| These Vernon shales are only hardened clays, without structure
and very easily decomposed.t_ They yield more readily to weather-
| ing and probably to erosion than any other rock, and the product of
| the ice rubbing was doubtless a lubricant and plastic paste essen-
| tially like clayey till in its mechanical properties. In consequence
| the hills of Vernon shale which stood within the zone of drumlin

| formation, in the conflict with the moving ice, were more easily
| shaped into the drumlin form than other rocks, but when given that
| shape they resisted the ice impact better than harder rocks. These
| shale hills were at the same time more compliant and more
| "resistant. They became drumlins in effect though not in origin.
| E They are erosional forms, while drumlins are constructional forms.

____ The soft Vernon shales» extend westward through the State but
nowhere appear so prominently at the surface as in the region

_ described above. Eight miles south of Rochester they are exposed

at about 570 feet altitude. It is apparent that along their east and

i)
II

1 The rapidity with which these shales weather to mud was the cause of dispute and litigation
in the matter of the deepening of the Erie canal afew years since. The contractors justly

| _ tegarded the shale as ‘

‘rock’? and charged for rock excavation ; but inspection afew months
_ later found the spoil banks to be only clay rubbish. :

i
,
|

| - -

416 NEW YORK STATE MUSEUM ss -

west outcrop they have been eroded by weathering and ice rubbing z
and the belt-of outcrop deeply covered with drift. Their more
common appearance on the Newark-Syracuse parallel is partly due 4
to greater thickness and also to the postglacial excavation by the ice ©
border drainage. The Salina shales as a whole, many hundreds of 4
feet in thickness throughout the drumlin area, have supplhed a large 4
amount of plastic and adhesive material for the drumlin con- q

struction process, and may bé one factor in the production of the

drumlins.

Concentric bedding. If drumlins are constructional forms, —
that is, were built up by a plastering-on process, then it should be
expected that on cross-section they would reveal some .concentric —
bedding or onion structure, with the upper layers parallel to the ~
drumlin surface. Theoretically the bedding need not be con-
spicuous as there could not have been great variation in the con- °
structive process, as compared with the work of water, in either j
kind or quality of material or in rate of deposition. The com-
parative uniformity in the work of the ice, taken in connection
with the heterogeneous character of the till;-would seem unfavorable

to any conspicuous structure.

Few cuttings in drumlins expose large sectional areas, and such ~
as do occur can commonly be seen only at close range, which 1s.
“unfavorable to inspection of indefinite and large-scale structures. —
To recognize the general structure it is necessary to have a com=- ©

prehensive view, yet not so distant as to obscure all details.

Bedded structure in drumlins has been casually noted ina few ~
instances but the only description of such feature (in the writer’s —

knowledge) has been given by Upham, of a few drumlins on the |

Massachusetts coast at Scituate and in the neighborhood of Boston, 3

which have been dissected by wave erosion."

The most favorable exposure of interior structure of drumlins q
known to the writer is found along the south shore of Lake Ontario, —
and specially between Sodus bay and Oswego. In this stretch of q
about 28 miles not less than a score of drumlins, many of large size, _
are dissected to their core by the wave erosion. The comstamey |
undercutting by the waves [pl. 8, 43-46] yields continually fresh ©
sections from top to bottom, and fortunately in different directions. —

Some drumlins are cut in direct cross-section; some in oblique ©

xz See titles on page 438 for the years 1888, 1889 and 1892.

\ Ya Nas
ayy
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XK
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cn

3 ; This area was molded by southeastward flow of the later ice,spreading from the Erie basin.

DRUMLINS OF CENTRAL WESTERN NEW YORK 417

~ section ; and some in longitudinal section. One could not reason-
_ ably ask for more favorable exposure than nature here affords.
The structure can not be seen properly at close range from the

- beach, nor at the long range from the steamers. In August 1905
the writer secured the help of an oarsman and with a small boat
examined the entire shore from Sodus bay to Oswego. Part of this
_ stretch was reexamined in September, and the study carried westward
from Sodus Pay Many photographs‘! were taken, some of which

The « erosion cliffs range in eae from 20 feet wp to 140 feciue ne
| growth of vegetation is rarely sufficient to obscure the structure, and
"in some cases is in itself a proof of the till bedding, as it lies in
, horizontal lines. The higher cliffs are all bare.

More than half of the cliffs show undoubted concentric bedaiae
| and in several it is surprisingly distinct. At distances which
S@eminimize the relief of the cliff faces, in buttresses, reentrants,
and amphitheaters [pl. 43], the fact of bedding parallel with the
§ drumlin surface is strikingly evident, and is shown in different
| ways. A difference in the texture of the beds is apparent even. “at
close range. Distinct zones or lines of boulders are often seen. A
| difference in shade of color is common, and the shading due to
| varying capacity for moisture is pronounced. The latter is also
_ shown by patches of vegetation clinging along certain zones. ‘The
| second cliff east of Sodus bay, © Cline’s bluff,” shows at even 2 miles
distance a conspicuous line of vegetation. A most striking proof
‘of bedded structure is shown by the differences in weathering, ©
which are often indicated, as in plate 46, by the uniformity in hight
on the cliff face of the conical buttresses. Two other cliffs which

show this feature well are: one east of Juniper pond and 2 miles east
of Fairhaven bay, which shows three lines of erosion cones; and

ithe first photographs were taken with an ordinary shutter which proved too slow with the’
_ tossing of the boat. These first photographs show clearly the bedded structure but they are too

blurred to be suitable for reproduction. For the second trip the Bausch & Lomb Optical

I) _ Company kindly loaned a ‘‘Plastigmat”’ lens and a ‘“‘ Volute”’ shutter, and the photographs of

j| pilates 43 to 46 represent an exposure of 1-150 of a second, in the hazy light of the last day of

‘September. The camera was a 5x7 Cartridge kodak, the only camera which the writer has used

six years.

_ When these views were taken the drumlin sections were very dry and the hygroscopic differe

nces in the till layers did not show as well as they do soon aftera heavy rain. Much better

ieéws can be obtained when all conditions are favorable, as quiet water of the lake, good light

418 NEW YORK STATE MUSEUM

another a mile northeast of the mouth of Eighteenmile creek and

about 5 miles southwest of Oswego. :

In cross-section view the concentric bedding decreases in con-—
vexity passing downward toward the bottom of the drumlin. In@
other words, the bedding near the base of the drumlin is quite
horizontal or slightly arched ; and the arching increases with hight
until near the top the layers are parallel with the drumlin pro-
file. In some instances, particularly toward Oswego, the sections §
exhibit a superficial bed, estimated at 10 to 20 feet thick, of a@
lighter color and yellowish shade, and apparently less compact
than the deeper blue-gray till. This superficial bed weathers into —
smoother or more uniform faces, instead of the projections, pinna- q
cles, towers, or battlemented forms of the deeper and harder till. ©

A good test, and a confirmation, of the concentric structure is
found in the oblique and the nearly longitudinal sections. A glance ~
at plates 7 and 8 will show how the lake erosion is cutting the drum- é
lins at very different angles. It is found that the stratification
exposed in these different sections has the direction which would
correspond to a concentric bedding. In sections approaching the —
longitudinal the bedding is quite straight and declines parallel with ~
the crest of the drumlin toward the tail of the hill. In general the |
upper beds are parallel with the cliff profile and have the curvature —
appropriate to the angle of the section. | |

The application of these facts of drumlin structure to the problem: ‘
of drumlin origin will be found in a later chapter. To facilitate the
study of the subject by any one who wishes to cxamine’the drumlin ©
sections for himself the following notes and directions are supplied. —

West of Sodus bay (the Pultneyville sheet) the cliffs are partly 4
morainal and only two good drumlin sections occur, one of them i
being shown in plate 46. East of Sodus bay the lake shore isa
included in the Sodus bay sheet, reproduced in plate 8, and the t
Oswego sheet, partly shown in plate 7. These maps show approxi- 7
mately the angle of the wave cutting with reference to the drum- |
lin axes. | | :

The drumlins which display the bedded structure in the clearest
manner are, taken in order eastward: Lake bluff (using the local —
names) [pl. 44]; Cline’s bluff, 1 mile east of Lake bluff ; Blind Bay —
bluff, 14% miles east of East bay [pl. 45]; two cliffs either side of
Juniper pond, which lies 2 miles beyond Fairhaven bay; and the

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DRUMLINS OF CENTRAL WESTERN NEW YORK 419

two cliffs midway between Eighteenmile and Rice creeks, southwest
of Oswego.

The best longitudinal sections are the one east of Juniper pond ae
the one halfway between Eighteenmile andkice creeks. hte: lighter
colored top layer is well shown in the three cliffs east of Port bay.

It should be understood that the distinctness of the bedding
varies with the degree of moisture and the lighting; and that it may
be subject to change with depth of cutting and so vary with time.

Formation: theoretical mechanics
Thus far this writing has been of a descriptive character with
only a modicum of reasonable inference. It is now time to take up

the philosophical side of the study and if possible explain the

origin and manner of making of the drumlins. In the earlier writings
on these structures the question of their genesis naturally received
much attention, but without confident conclusions. Probably no
geologist doubts their glacial genesis but the precise manner of their
formation has been in question. ‘Two general views have been held,

Some that they are overridden and reshaped moraine. drift, the

other that they are constructional forms, built up ab initio by the
moving ice out of its ground moraine or interglacial drift. That they
received their form by the molding effect of the overriding ice sheet
seems too evident to be questioned.

The idea that drumlins were primarily moraine masses may be
true of some drumlins, and possibly of some forms in New York;
but it certainly does not apply to them in general. The Tengen
of the drumlins is not in accord with the theoretical location of any
former morainal belts; and this conception takes no account of
isolated drumlinsin some regions, or groups of drumlins far removed
from suggestions of other drift masses. Moraine deposits are
expected to lie in continuous belts. Furthermore, no moraines of
such breadth and quantity of drift as are held in the Rochester-
Syracuse drumlin area are found in New York, probably not in the
Eastern States.* -

1It should be admitted that the full history of the ice work in New York and New England
is doubtless more complex than we now realize, and that probably there was ice invasion with
its attendant frontal waters previous to the Wisconsin epoch, We now see the deposits as the
last ice sheet left them, and while we must take the phenomena as we find them and study
them as they lie we must not ignore the probability of an antecedent and different condition.
However, it would be unscientific to minimize the facts before us and magnify the unknown or
theoretical features,

420 NEW: YORK STATE MUSEUM

Considering the great volume of water-laid drift commonly
associated with the New York moraines, amounting in many cases
to almost the entire mass, it would seem certain that the drumlins
in the same territory, if overridden and reshaped moraines, should
frequently if not habitually hold sands and gravels as a part of their

mass ; in other words they should haye the irregular structure and

miscellaneous composition of the moraines. Indeed it would seem
likely that with the volume of deep-seated waters in the marginal
portions of the ice sheet (the streams either subglacial or in deep
trenches) aqueous deposits might not infrequently be left beneath
the ice in such position as to be incorporated into the drumlin mass.

However, as stated above [p. 412], this feature is remarkably rare. —

Drumlins may be built on other antecedent drift, and stream or lake
deposits may occur on their surface, but the drumlin material in the
area under discussion is very compact till, and may be distinctly
bedded. | aie | eae vee
The facts pertaining to the drumlins of New York are only con-

sistent with the theory of their constructional origin. And now

we have the sufficient proof that at least a great number of thenr
were slowly built up by a plastering-on process, as described above
[p. 416]. |

Since we know that the Sodus bay-Oswego drumlins are con-
structional it is a legitimate assumption that other drumlins in

contiguous areas have the same origin. In the further discussion ~

of the New York drumlins their constructional origin will be

assumed.!

In the theoretical discussion of the mechanics of drumlin con- |

struction three sets of factors are recognized: (a) those pertaining to
the ice itself, (2) those relating to the drumlin-forming drift, and (c)
the external influences of topography and climate. These will be
briefly considered in the above order.

a Dynamic factors pertaining to the ice body :

1 Vertical pressure, which is directly proportionate to the vertical
thickness of the ice sheet. ae

2 fHortzontal pressure. At the periphery of the continental ice
sheet the horizontal pressure necessary to produce flow on level

1 Since these lines were written it has been found that sections of drumlins in Oakfield

cemetery, Syracuse, exhibit excellent bedding.

ie |

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DRUMLINS OF CENTRAL WESTERN NEW YORK 421

ground or on an up slope (as in the New York drumlin area) was
mainly an effect of the vertical pressure in the deeper and rearward
part of themass. The depth of the ice sheet along the drumlin-
making zone was probably insufficient to greatly aid the forward
movement; but to the degree that plasticity was effective the
vertical pressure might have had some effect in modifying the
movement or in producing differential flow.

° Vigor and velocity of flow. This is due primarily to the thrust
from the direction of the deeper ice. The horizontal displacement
or mass movement of the ice would be influenced by the larger
features of the land surface and by the local temperature and
rainfall [see c].

4 Differential flow. The practical plasticity of the ice would

theoretically seem to allow unequal flow, or a tendency to flow in

prisms or currents analogous to stream currents; and the drumlins
are evidence of such local variations in the ice work.

5 Plasticity. This property of glacier ice would probably be
increased by pressure, heat and water supply as a lubricant. In the

marginal, drumlin-forming zone of the ice sheet plasticity due to

vertical pressure would be reduced, that due to horizontal pressure

_ would be fairly constant, while that due to heat and rainfall perhaps
would be increased.

6 Factors relating to the drift held in the ice

1 Volume of the drift. It has been recognized that plastic flow of
glacier ice diminishes with increase of rock debris. But the move-

_ ment of the lower ice by rearward thrust would not be so greatly

affected by the contained drift. The influence of the drift toward
rigidity might assist in producing differential flow in prisms or bolts.
Whatever might be the effects on the flow of the ice by variation in

the load of drift its abundance in the lower ice would seem to be a
_ direct aid to drumlin building.

2 Position of the drift. The vertical location of the rock rubbish
in the ice seems an important factor. Debris superficial to the ice

sheet could only produce morainal masses. Drumlins must have

been built from the debris carried in the lower layers of the ice. _

3 Quality of the drift. It would appear that a clayey, adhesive
character of the drift would facilitate the plastering on process, by
which the New York drumlins are certainly made. No drumlins
are found composed largely of boulders and friable material.

422 NEW YORK STATE MUSEUM

c Factors of external control

t General land slope. A down slope would favor movement of the : 4
ice both by thrust and by plastic flow of the upper over the lower

layers. An up slope would probably retard or prohibit motion at
the bottom except by thrust. The great drumlin area of New York
has an up slope, but the dominant minor area is nearly level. The
Chautauqua drumlins are on high ground, very irregular but broadly
level. | |

2 Minor topography. This factor is indefinite and uncertain

because variable in many ways. It would seem that great irregu-
larity of the overridden land surface would be unfavorable to move-
ment of the lower ice, and the drumlin-making motion would lie
more in the plane of the hilltops. (This has a bearing ‘on the con-
struction of the Syracuse island masses, page 425.) Small promi-
nences in the bed of the ice sheet might be favorable as nuclei for
the initiation of drumlins.

3 Temperature and water supply. Plasticity of the ice would be
favored by heat and water. . Cold and dryness favor rigidity. The
margin of the ice sheet must have had nearly the highest possible
temperature and the largest supply of lubricating water, from rain-
fall and ice melting. This would be quite independent of latitude
as the ice can not be warmed above the melting point.

It is apparent that the drumlin-building process involves many
factors, and most of them indeterminate. The problem is exceed-
ingly complicated, including not only the difficult subject of the
behavior of plastic solids but the action of. the plastic ice under a
complexity of geologic conditions.

Drumlin forms and observed relations. ‘he interaction of

the physical and geologic factors noted above has produced a great
variety of drift forms which we may include under the general class
of zce-molded, or drumlinized drift. ‘These forms have been described
or noted in the writing above, but it is well to name them here for
comparison.

1 Domes or mammillary hills and low broad mounds.

2 Broad oval drumlins [pl. 7]. ee

3 Oval drumlins of high relief [pl. 11].

4 Long oval drumlins, commonly bolder on the north or struck

end; the dolphinback or whaleback hills [pl. 14].
5 Short ridge drumlins [pl. 6].

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DRUMLINS OF CENTRAL WESTERN NEW YORK 423

6 Long ridge drumlins. This includes two extreme varieties of
form: (a) the long broad ridges or rolls or gentle swells which.
are not generally recognized as belonging in the drumlin class,
and commonly fail of representation on the contoured maps
[pl. 18]; (2) the small, close-set, parallel ridges which lie as
minor moldings between the larger and conspicuous ridge
drumlins, or those which form the attenuated edge of a
a drumlin belt [pl. 13]. ,
a7 Sorupt struck slopes [pl. 30, 35, 4o].

_ 8 Low or gentle struck slopes [pl. 22, 23].
E; Sharp crested hills with steep, or even concave, side slopes
mpl 20.|
x Many occasional or peculiar forms and characters might be noted
but they are not regarded as genetically important.
E,. Beinve relationships of the several forms are not so definite or exclu-
sive as might be expected, though further study may discover new
_ facts. However, there are certain broad relations of distribution
and association which will be restated here.
_ 1 The drumlin area is practically restricted to the north-facing or
-ice- opposing slope.
_ 2 The region of greatest development of drumlins is on the low

Ontario plain, which is nearly level. |
3 The greatest development lies over the greatest thickness of the
| ‘Salina shales, or where the drift is most clayey and adhesive.
; aw he predominant drumlin area lies where the ice flow was east
of south and at a high angle with the general southwesterly flow.
4 a The somewhat exclusive development of the long and low ridges
(6 a) is in the northwest corner of the State where the ice had only
th le one direction (southwest) of flow, but where there was less”
; volume of clayey drift because less thickness of eroded shales.
6 The individual drumlins are not placed in any orderly sequence
or regular disposition, but are irregularly spaced.
3 7 Within the same belt of drumlins or what is regarded as a forma-
tional unit the south forms or those nearer the ice border are more
attenuated, while the north forms or Uhose under the deeper ice are
broader.
8 A belt of moraine drift lies in front of the attenuated border of
fhe drumlin belt.
9 The greater hight of the drumlins, their steepness of slope and

424 NEW YORK STATE MUSEUM

regularity of form seem to occur in the middle of the belt and to 4

characterize the maximum work of the constructive process. . ;
ro Steep struck slopes seem to be more commonly associated with” q

the steep and long ridges; while the low struck slopes pertain to the

lower and broader forms.

Relation to moraines

The precise relation of the several drumlin belts to the terminal g
(recessional) moraines can not be fully stated until further arc
study has been given to the moraines, but a few interesting facts can
now be given. m

If the drumlins specially represent the more vigorous movement —
of the bottom icé during episodes of either frontal advance or halts _
in the frontal recession then each drumlin belt should correlate with —

a frontal moraine.t. Such relationship seems definite for the central —

or main drumlin belt, the Oakfield-Syracuse series, in the stretch -
from Syracuse westward as far as the meridian of Rochester. Where
the drumlins fade out to the attenuated forms, from Auburn west-
ward to Geneva, a distinct moraine lies 2 or 3 miles in front, on the 4
south [pl. 13]. Remnants of the moraine mark its course eastward —

to Split Rock, southwest of Syracuse, but in the Split Rock district
the ice front was swept by rivers of ice border drainage and the ice-
rafted drift was largely dropped into the grasp of the streams. West |
of Geneva tlie same relation of drainage to the ice front is very pro- _ |
nounced. A remarkable series of strong river-cut channels extend- — |
ing from northwest of Batavia eastward to Phelps swept the ice 4
margin and removed most of the terminal drift.) thong some — ;
remnants are left, sufficient to prove its position.? BE q

The interesting fact in this connection is that the drumlins of the .
main series reach in full strength up to the north bank of these |
channels [pl. 9, 11, 14] and there abruptly end. The drainage chan-
nels do not represent the forward position to which the ice would. 4
have reached with no interference (or the location of the moraine | 4

t The theory is now held by glacialists that the front of the continental glacier receded by
oscillation, a succession of retreats and lesser readvances, and that the stronger moraines were -
accumulated at the ice margin during the culmination of the advances. The successive moraines ;
in any given area are thus supposed to mark the successive readvanced positions of the ice front. . - |
For this subject see specially the writings of F. B. Taylor, ‘‘ Moraines of: Recession and Their a
Significance in Glacial Theory ” (Jour. Geol. 1897: 5: 421-66]. : . gy 1

2 The description of these glacial river channels will be found in another bulletin of the State ~

Museum, under the title, * Glacial Drainage between Batavia and Syracuse.” e

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DRUMLINS OF CENTRAL WESTERN NEW YORK 425

1 such case) but a belt further iceward, the rivers truncating the
inner border of the ice sheet.
oraine belts like the Auburn and Seneca Falls moraine represent

sively dropped at the extreme margin, while, pari passu, the
alins were forming beneath the ice in the rear of the moraine,
the subglacial (and perhaps the lower englacial) drift.

lows between them. Not infrequently we find a patch of irregular
‘surface among the drumlins which can readily be discriminated and

mlins [see p. 412] as in the Junius kame area. Sometimes the vol-
e of moraine drift increases to the north and is so distributed as to
e a decided morainal surface among the northern drumlins, as in
Walworth district [pl. 15]; or else the next succeeding moraine
the north laps on to the north edge of the drumlin belt, as in the
wego district [pl. 6].

\t the termination of heavy lines of glacial drainage, during both
active and the stagnant episodes, heavy deposits of water-laid
ft (kame moraines) accumulated, as the Junius, Victor, Ironde-
oit valley, Mendon, and other kame areas.

‘heoretically the moraines should be weak where the drift was
tin drumlin form, and the facts seem in accord. In the stretch

ame areas are strong.
Special features

_ Syracuse island masses. These remarkable groups are partly
shewn in plates 9 and ro and are fully shown on the Syracuse and
aldwinsville sheets. They are partly bounded by river channels of
latest glacial drainage cut in Salina shales. North of Warners
pl. g| is an example of such drumlin massing not surrounded by
river valleys. In the more striking of these groups there 1s a cumu-
on or increase of hight toward the center which is a peculiar
ture. iiemenese drumilin masses have a core of rock reaching
ove the Salina shales, which form their base up to 500 feet or
e; it has not been found, though it is not improbable for the
re northerly groups. : |

| Batavia to Syracuse the moraine belts are weak, though a few _

426 NEW YORK STATE MUSEUM Bas

The isolation of these groups can not be entirely due to channel- _
ing by the later drainage because the drumlins which cap the island- j
like rock masses are not themselves eroded, but lie wholly above the ~
plane of the river work. It appears as if the ice rubbing did not —
touch the lower levels but was confined to higher planes. The forms 4a
do not seem explicable on the postulate of a single ice invasion with ~
one episode of correlating ice border drainage. The relation of the —
drumlins to the erosion, and the character and direction of the stream ;
courses [pl. 9. ro] suggest a complicated history. We have here only ~
one of several groups of pheromena which argue for more than one
ice epoch with their correlated stream work. 7 q

Montezuma island groups. Plate 12 shows the largest of sey- —
eral groups of drumlins which rise out of the marshes that occupy —
the low ground north of Cayuga lake. These are not conical or
cumulative masses like those described above, but isolated groups, ©
of irregular forms and sizes, even down to single drumlins. In the
Montezuma district these groups or individuals rise out of the broad _
marshes as if half drowned. A few small knolls are mapped about
the borders of the marshes, like the summits of nearly buried drum- Bf
lins, but it does not seem likely that the absence of drumlins over ~ |
wide tracts could be due to entire burial of drumlins under lake and
vegetal accumulations. More likely the marshes are only the low @
areas similar to others at higher levels that are destitute of drumlins. ca
This leads to the next topic. : Rhy ge

Nondrumlin areas: open spaces. The broad swamp tracts, —
like the Montezuma marshes, belong in this category as well as more

elevated and drier areas. An example of the latter hes north of ©
Clyde, where a large tract im the center of the, Clyde quadrangle 4
shows white on the topographic sheet. The east edge of this tract ©
is shown in plate 3, figure 3. This surface was under Iroquois waters
but the lack of drumlins is certainly not due to their destruction. —
Evidently they were not formed in thistract. The reason is obscure,
since the area is irregular in shape with scattering drumlins on all
meridians and close set on the west, east and south. This absence ~ 4
of drumiins over considerable tracts in the midst of heavy develop-
ment is more difficult of explanation than the formation of the =
drumlins themselves . =

These puzzling features lie in the region of deep drift filling of. >
ancient valleys, the northward continuation of those now holding a

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-DRUMLINS OF CENTRAL WESTERN NEW YORK 427

the finger lakes, and chiefly in the north and south depression of —
Sodus bay and Cayuga lake. The nondrumlin spaces can not be
regarded as having been occupied by stagnant ice during the

-drumlin-shaping episode since they. are surrounded by drumlins,

and are comparatively free from moraine. They can not represent
areas of ice movement too vigorous for drumlin accretion or shaping

_as the ice along the line of flow must have had a practical equality

of motion. There is no reason for supposing that there was any
lack of drift, since an immense quantity is piled in drumlins imme-
diately southward. The location and distribution of the spaces, as
well as the drumlins themselves, are such as to oppose the idea that
the drumlins represent an original morainal distribution of earlier
drift. We have to recognize the probable equality of the drumlin
and nondrumlin loci in the elements of depth and pressure of the
ice, in its impact and velocity of motion and in its burden of drift
The following suggestions are offered toward the explanation of
these puzzling features. In the region of deep valley filling it is
possible that some depressions were below the average level and

consequently below the plane of the more vigorous thrustal motion,

and it is conceivable that a plane of shearing might have been estab-
lished above the depressions. Shearing once established would

_ probably be unfavorable to the initiation of drumlins, as the drum-

lins imply some degree of local drag in the bottom ice during the

_time of accretion or shaping of the forms. The lowest of the open

spaces have been partly filled with lake silts and stream detritus and
vegetal accumulation, and some are still partly under water, as the
Montezuma marshes; but the spaces north of Clyde do not appear
to have been leveled by postglacial agents. The existence of well
developed drumlins within or on the borders of open spaces might
be due to accretion on existing obstructions, while the shearing
tendency discouraged initiation of new masses.

A second suggestion is based on the idea of a complex glacial
history. An earlier ice invasion may have localized and heaped
the drift in part, while the interglacial stream work carved broad

_ channels through the area, which the latest ice work has not wholly

obscured.

Channeis among the drumlins. These are connected with or
blend into the open spaces discussed above and are part of the
same problem, They are specially developed between Fairport and

428 NEW YORK STATE MUSEUM

Lyons; between Montezuma and Syracuse; and along the Seneca

river. Those with direct east and west course were occupied by the

latest ice border drainage but apparently were not wholly produced
by it. These features appear on the Macedon, Palmyra, Weedsport
and Syracuse sheets, and a suggestion of them is shown in plates

g-12. The channels all lie in Salina shales and possibly they have

some genetic relation to the erodible nature-of the rocks.

The existence and location of these low, continuous passages are

strikingly emphasized by the remarkable windings of even the larger
streams, Seneca river for example. The northward turns which this
wayward stream makes east of Savannah, and more strikingly from
Cross lake (an open tract) around by Baldwinsville and south to
near Onondaga lake, must have been found open or the stream
would have taken the direct eastward passages that are almost as
low today even without any postglacial erosion. A smaller illustra-
tion is found in the case of Ganargua creek east of Palmyra, where
it deserts the open glacial stream course and wilfully turns north
around by East Palmyra in a constricted and uninviting pass, and
repeats the act with less excuse northeast of Newark.

One suggestion for these open passages, which were certainly left
open by the ice removal and were not cut by postglacial erosion, is
that they were made by. subglacial drainage, either under free flow
or under hydraulic pressure. This seems reasonable for south-
leading passages like those northeast of Clyde, and even for north-
leading channels of gentle grade, like the valley of Dead creek in
plate 10; but it is not satisfactory for the east and west passes which
were transverse to the ice movement.

Another suggestion is that the passes were cut by glacial drainage
of an earlier ice sheet, with modification by the subsequent inter-
glacial erosion: It seems probable that the complex history of the
region may involve such episodes and activities; or that perhaps the

oscillations of the last (Wisconsin) ice sheet were sufficiently exten-

sive to produce the phenomena. The difficulty under this theory is
to explain why the drumlin-making work of the ice did not rub the
channels full of drift. This difficulty is of the same kind, however,
as the absence of drumlins over interdrumlin tracts. In the case of
the deep channels around the Syracuse island masses it might be
suggested that possibly during the latest stage the channels were
occupied by stagnant ice over which the drumlin-forming layers

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DRUMLINS OF CENTRAL WESTERN NEW YORK 429

i. moved or slid by shearing; but this could hardly apply to the Clyde
and Montezuma districts, where the drumlin forms lie at the lowest
levels. :

A modification of the subglacial drainage theory offers some help. 7
| It seems probable that the last stage of the glacier in this region left
an extensive border tract of stagnant ice, and that unequal melting
duetoa variety of causes produced detached blocks or tracts of ice
around or among which the copious glacial waters excavated many
& channels. The subglacial drainage combined with the later inter-
ice block drainage may largely account for the peculiar features.
In this connection it must be understood that the attitude and
' elevation of the land surface of the region has changed to some
extent since the features were made; and that the lakes and slug-
gish waters, aided by organic growths, have partially filled the low
grounds.

Summary

Age of the drumlins. The form and relations of the drumlins
_ in the Pulaski district, due to the change of direction in the ice flow
proves that they were shaped during the latest phase of the ice work
in that locality, and not during any earlier stage. The same conclu-
sion is reached by the theoretical considerations and enforced by
the facts of observation for the entire drumlin area.

The peculiar distribution of the drumlins and their orientation _
r, prove that they were shaped by the spreading flow of the semistag-
nant ice mass reposing in the Ontario basin. The correlation of
moraines and of ice border drainage channels with the attenuated
edge of the main belt of drumlins indicates that the drumlins were
formed beneath the border of the ice sheet. This correlation of the
drumlin shaping with the latest work of the ice in the drumlin region
_ has been noted in other drumlin areas, as Wisconsin, Massachusetts,
Ireland and Germany. ‘The fact seems to be sufficiently established
_ that the alinement and shaping of the drumlins was given under the
_ waning border of the ice sheet, at least in the case of the continental
glaciers. — :

Thrust motion of the ground contact ice. Drumlins are

shaped by the sliding movement of the lowest ice, that in contact with

_ the land surface. This fact implies that the whole thickness of the
L Bice sheet participated in the motion. Such motion was not due to
gravitational stress on the ice mass over the drumlin area, because the

430 _ NEW YORK STATE MUSEUM

general slope of the drumlin area is up hill, but was produced by an
effective thrust on the marginal ice by the pressure of the rearward
mass. As the ice sheet thinned by ablation there came a time when
the drift-loaded ice in contact with the ground was subjected to less

vertical pressure and to relatively greater horizontal pressure by the |

deep ice in the rear, and was pushed forward, bodily. In this fact is
believed to lie the key to drumlin formation.

It does not follow that drumlins must always have been formed
where the bottom ice had a sliding motion, as several other condi-
tions are probably requisite, but. it seems quite certain that long-
continued and vigorous horizontal thrust is the prime necessity.
Such thrustal movement would be effective only where a border of
the ice sheet was backed by a thick or vigorously pushing rearward
mass. The combination of conditions requisite for effective thrust
movement over a belt of country and for thé considerable time
necessary to build up the drumlins may be rare. It does not seem
so strange that drumlins are uncommon features of the drift when
we add to the requisite dynamic factors mentioned above the several

others which are oebdless directly concerned with the drumlin

formation.

As a working hypothesis it may be assumed that wherever the

ground contact ice had a vigorous movement of some duration it
should be indicated by the molding of the ground surface, specially
where that surface is comparatively smooth and composed of drift
or soft rocks. The form and degree of the ice molding would vary
according to the strength: and adjustment of the several factors.
An application of this idea can be made to the region under
present study. ‘

Well marked drumlins are not found on the high eround east of
Seneca lake, and are wanting on the low ground east of Syracuse.
The explanation seems to le in the relationship of the larger topog-
raphy to the movement of the ice sheet. When the glacier was deep

over the Finger lakes region the bottom of the ice inthe drumlin 7

area was probably quiescent and served as the’ bridge over which

the upper ice moved.by gravity; the repose of the lower ice probably —

being due to the opposing land slope and to the large volume of
drift which the ice had incorporated. Over the nearly level area

north of the Finger lakes the waning of the ice sheet finally sub--

jected the ground-contact ice to a vigorous and long-continued hori-
zontal thrust with consequent sliding motion, But in the adjacent

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DRUMLINS OF CENTRAL WESTERN NEW YORK 431

district of low ground northeast and east of Syracuse (over Oneida
lake, Canastota, Oneida and eastward) we have an illustration of
nonmotiort of the ground-contact ice. The almost bare hills of soft
Vernon shales in the region of Canastota have not been subjected to
the rubbing action of the ice from any direction. In form these clay
hills closely resemble moraine drift, and with their slight veneer of
glacial rubbish would at first be mistaken for moraine by even the
experienced geologist. This surface would have been sensitive to
any ice movement, the absence of which is explained as follows:
While the ice sheet was thick the flow was from the northward and
the ground-contact ice in this district, lying in the broad depression
between the Adirondack massive on the north and the high plateau
on the south, was quiescent. With the waning of the ice sheet it
disappeared from the high ground to the north so that the stagnant
mass resting on the Canastota-Oneida district was not subjected to
any push from the northward. During the closing or drumlin-mak-
ing phase of the ice work in the Ontario basin the radially spreading
ice of the Ontarian mass did not reach this district. In brief, the
ground-contact ice over the Canastota-Oneida district, although occu-
pying a low tract on the edge of the drumlin area, did not at any
time receive horizontal impulse but was deserted and allowed to
quietly melt away, or perhaps to be lifted and rafted off in the
glacial lake waters which fronted the glacier. The extreme reach
of the drumlin-forming activity in the Syracuse district was in the
form of a tongue or wedge of moving ice which was thrust south-
eastward along the Onondaga lake depression and over the site of
Syracuse, ending a few miles southeast of the city; and affecting only
the higher ground, or the summits of the island masses.

Origin. It is certain that the New York drumlins were con-
structed or built up by a plastering-on process. The ice did not
drop its drift burden in the depressions or low places but plastered
it on the obstructions. ‘The plastic and adhesive character of the
shale-derived drift of central New York is probably one factor
accounting for the great number, hight and shape of the drumlins
of that district.

The rocdrumlins, or shale hills with the peculiar drumlin form,
being shaped by a moderate amount of erosion of the soft rock
might suggest, at first thought, that erosion was the main factor in
drumlin formation, Possibly it may be in some regions; but vig-

432 NEW YORK STATE MUSEUM

orous abrasion of hard rocks would sare be consistent with
drumlins in the same locality.

The building of drumlins by the plastering process was Coleen
with a rubbing off and shaping effect. As masses or hills the drum-
lins were produced by accretion of the drift, but their peculiar form is
due to the erosional factor. The whole process may be compared to
the work of the sculptor on a clay model: a plastering on and rubbing

away. The accretion was due to the greater friction between clay

and clay than between the clay and ice. The hills of accretionary
drift resisted the ice impact and rasping effect just as did the hills
of shale. The form possessed by both classes of hills is that which
opposed successful resistance to the ice erosion, and the least resist-
ance to the ice movement. : .

Dynamics. It seems evident that in the typical drumlin area the
ice did not move as a solid mass or even in wide sections, for such
motion should produce a planing or leveling effect, such as is illus-
trated in the Niagara-Genesee prairie [pl. 19]. The drumlins are
proof of a plastic flow or yielding of the ice; while the long, straight
ridges suggest that the ice was pushed in comparatively rigid bolts
or prisms that wavered and shifted. .

In the balancing and adjustment of the several dynamic factors in
the drift-burdened ice the two opposing forces of rrgidity and plas-
ticity seem to be the most important. The amassing of the drift into
drumlin form, or at least the nonremoval of the hills, implies that the
depth of ice and the vertical pressure were so moderate as to allow
the plastic ice to override and adapt itself to the hills, while at the
same time the whole sheet of ice was sufficiently rigid to move
under horizontal thrust.

Judging from the facts and theoretic mechanics noted above it
would seem that the drumlins represent the short lines of temporarily
diminished pressure and of lagging flow. These lines of variable
pressure and motion, though close set in the dominant drumlin area,
must have been discontinuous, short and constantly shifting. Drum-
lins could not have been determined, as regards location at least, by
external influences, as atmospheric agencies above or topographic
and geologic features beneath, but must have been produced by the
interaction of the mechanical factors resident within the ice itself,
the latter moving as a plastic solid. Their initiation may have been

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DRUMLINS OF CENTRAL WESTERN NEW YORK 433

due to some obstruction beneath the ice or to a local amassing of
‘drift by the ice itself.

Drumlin forms. The breadth of the Oakfield-Scottsville-Pal-
myra-Syracuse drumlin belt or series, which is supposedly a unit in
time of formation, is about 20 miles wide in the central part. The
eastern Ontario series has about the same width on the Fulton sheet.

If the northern and broader drumlins in each beit were mostly
built contemporaneously with the southern attenuated forms, as
seems most probable, then we may assign a few of the conditions
that were responsible for the different forms.

The northern, broader and more widely separated drumlins, such
as those at Sodus [pl. 4], were certainly under greater vertical
pressure on account of the greater depth of the ice. This might
have given greater potential plasticity, though the effective plas-
ticity and the differential movement might have been less than in
the central part of the belt. On the other hand the attenuated

:. drumlins [pl. 13] under the thinner ice near the border of the

“sheet would be subject to less vertical pressure. Here the ice had
less frontal resistance and therefore freer movement; it was less
burdened with drift, having already built the drumlins in the rear;
and probably it had less effective plasticity and less differential
movement. In other words, the attenuated, border forms of the
drumlin belt were formed beneath ice moving with relatively greater
freedom, greater relative rigidity, and with more uniformity and
continuity.

~The culmination of the drumlin-making process seems to have
been m the middle of the belt, where the several dynamic factors.
were well balanced and were working together at the maximum of
efficiency. There the drift was abundant and plastic; the rigidity
and the plasticity of the ice were active but well balanced; and the
differential flow was at its maximum, that is to say, the ice was not
moving in long, rigid bolts or wide masses but in short and wavering
prisms. }

The very long and flat ridges characteristic of the Niagara-Genesee
prairie [pl. 18, 19] seem to be the product of steady and long-con-
tinued movement of thicker and more rigid ice than that which built
the shorter, steeper and crowded drumlins in the middle of the State.
The ice probably had less burden of drift, less differential flow and
less effective plasticity. The effect was similar to the production of

434 NEW YORK STATE MUSEUM

the small, linear forms on the attenuated drumlin border in the

Waterloo-Seneca Falls district, but the work was on a much larger
scale. The direction of the drift molding in the western district, it

should be noted, is that of the prevailing direction of the continental

glacier over the region.

Depth of the drumlin-making ice. We have no conclusive
facts on this topic but some suggestive data. The relationship of
the Waterloo-Seneca Falls moraine, and of the ice-border drainage
channels on the west, to the south edge of the main drumlin series
seems to locate definitély the edge of the ice sheet during that
episode. North of the Finger lakes region the receding ice front
was continuously bathed by glacial lake waters, and the moraines
were laid down under water. The moraine above named seems to
correlate with certain deltas and outlet channels to the east. If the
correlation is correct the water in which the moraine was deposited
had a surface altitude, present elevation, of about geo teet, Wie
depth of water at the ice front was therefore about 4oo feet, since
the moraine tract lies at about 500 feet.

As the moraine is weak, largely because the drift load had been
incorporated into the drumlins in the rear, we may assume that the

ice was not heavily anchored in the lake water by its load of rock ©

rubbish. In order to retain its place under the buoyancy of the

waters it must have been at least 450 feet thick, or 50 feet above |

the water. Taking this as the minimum depth of ice at the glacier
margin and assuming a surface slope of 30 feet to the mile, the eleva-
tion of the surface of the glacier over Clyde, 12 miles nershpotemme
moraine, would be (950+30x12) about 1310 feet. Since the general
base of the Clyde drumlins is about 400 feet elevation the depth of
ice in the center of the drumlin belt was about goo feet. The drum-
lins are less than 200 feet high, which gives a depth over their tops
of more than 700 feet of ice. This is merely suggestive.

Complex history., It is very likely that there are undiscovered
and unsuspected elements in the Pleistocene history of central-
western New York, and that it is much more complicated than it
now appears. Probably there has been more than one epoch of ice
invasion and retreat along with heavy erosion by glacial and non-
glacial waters. As we see the drumlins today they represent in their
forms, in each series, the latest ice work; but it is quite possible that
some of them were related to an earlier ice sheet.

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5 Box, lee. eg Rae, } S Korma |

en are Or ane = Cuaureeaas we / bo oe 2. oo “a if %, nee \
Faujhrek | ‘ sy of ase Pop ne es | eee Tose Pd of 7 » ty, \
: et hese Sh Ae A . ‘\. -aee SR OS Ns ae Nip as bait oe el

Druinlins of Iar-Connaught, Treland
Reduced from portion of the map published by Kinahan and Close

mile.

®

DRUMLINS OF CENTRAL WESTERN NEW YORK A35

Drumlins of Ireland

The remarkable series of drumlins described by Kinahan and
Close? haye a special interest in this study, as they are the type
forms, produced by local glaciation in a far distant land, and are
strikingly similar in essential features to our New York forms.

The distribution of the principal group of the Irish drumlins is
shown on plate 47 which is_a copy, in reduced size, of a portion
(upper right corner) of the original map by the Irish authors. The
direction of flow of the ice current that produced this group of drum-
lins was toward the north, and spreading specially to the west, toward
Clew bay; but in other districts the few drumlins have other direc-
tions, corresponding to the radial flow of the ice away from the local
center of accumulation. The arrangement of the drumlins in curv-
ing lines of the ice flowage is very striking, and not easily explained
except by the constructional theory of their genesis.

The drumlins are described as occurring only on low ground, and
even forming islands and shoals in the sea (Clew bay). Their
absence from some parts of the low plain is noted as a feature not
understood.

The up stream ends of the drumlins (with reference to the ice
currents) are noted as the blunt ends, althougn this is not stated as
a constant feature, since the hills have suffered some erosion by
marine submergence.

The “parallel shaping” of the general ground surface in the
drumlin district was observed.

The extreme hight of the drumlins is given as 180 feet,- in
striking accordance with the New York forms. Another important
observation is the “ observable uniformity in size in the same neigh-
borhood.” Concerning length it is noted that several of the drum-
lins are 2 miles long; and that the mean length is not less than %

With reference to the composition the authors say that the drum-
lins “consist of stiff, unstratified boulder clay, containing well
pitied sand scratched stones and blocks.” “They have -beén

——

t Kinahan, G. H. & Close, H. M. General Glaciation of Iar-Connaught and its Neighbor-
hood, in the Counties of Galway and Mayo. With map. Dublin 1872.

For the favor of seeing this somewhat rare pamphlet and using its matter and map the writer
is indebted to Mr F. B. Taylor.

436 NEW YORK STATE MUSEUM

unquestionably formed by some operation different from, and ante-
cedent to, that which produced the water-arranged gravels and 7
eskers. Deposits of water-formed gravel, etc. , clearly of later date, 4
often occur in the lower ground between the drumlins, and even
banked up against them.” 3

The authors apparently regarded their drumlins as constructional
forms and did not regard the matter as needing discussion, since ~
they refer to the origin of the drumlins only incidentally, as follows:

“ No agent which can not do both kinds of work, rock-scoring and
drumlin-heaping, can be proposed as having caused them” [p. 9].

“; 3. Amd ithesstormedsiine drumlins by an operation evidently 3
similar to that by which a stream of water often makes longitudinal 4
ridges of sand in its bed.” ,

Bibliography

The following list of writings in English relating to drumlins is
not exhaustive, and it is possible that some valuable references have
been overlooked, specially of. foreign authors. Numerous incidental

references have been purposely omitted. Outside of English the ~

literature seems scanty, but an important paper in German is noted
on pase 394: , 3
Persons unfamiliar with the phenomena of drumlins might well
begin the study by reading the paper by W M. Davis that is given
as his fourth title in the following list; and later the papers 7 4 ;
Warren Upham for the years 1889, 1892 and 1893. @

Barton, G. H. Bost. Soc. Nat. Hist. Proc. 1892. 26: 23-25. , Ai. a :

6: 8-13. :
Bonney, T. G. Ice-work, Past and Present. 1896. p. 116-19.

Glacial Origin of Channels on Drumlins. Geol. Soc. Am. Bul. 1894.

Chalmers, Robert. Geol. & Nat. Sur. Can. An. Rep’t. n. s. 1888-89. 3 |

p. 23.N:;
Chamberlin, T. C. U.S. Geol. Sur. 3d An. Rep’t. 1881-82. p. 306,
Geol, Was.) 188g. si: 2oge Se ty )
——— Am. Ass’n Adv. Sci. Proc. 1886. 35: 204.

——— Horizon of Drumiin, Osar and Kame Formation. Jour, Geol. 1893.

I: 255-67, 521-24. .

—— Am. Geol. 1893. 12: 176.

— Geol. Soc. Am. Bul. 1895. 6: 216. »

— The Great Ice Age. Ed. 3. 1895. p. 743-45. (James Geikie)
—— & Salisbury, R. D. Geology. 1906. 3: 360.

4

ET

£5 RGR ERE SNP ERT Ta

DRUMLINS OF CENTRAL WESTERN NEW YORK 437

Close, H. M. On the Glaciation of the Rocks near Dublin. Roy. Geol. Soc.
trelgnd=. Jour. -1864.° 1:3.

Notes on the General Glaciation of Ireland.

Roy. Geol. Soc. Ireland.
Jour. 1866. 1: 207.

oyeGeol soc. Ireland. Jour. 1877. 5:49:

Dana. Am. Jour. Sci. 1883. ser. 3. 26: 357-61.

Davis, W.M. & Shaler, N.S. Illustrations of the Earth’s Surface; Glaciers.
eeresi., Text describing plate 24.

osm soc. Nat. Fist. Proc. 1883. 22:34, 40-42,

Drumlins. Science. 1884. 4: 418-20.

The Distribution and Origin of Drumlins. Am. Jour. Sci. 1884.
ser. 3. 28: 407-16.

mastesoc. Nat. Hist. Proc. 1803. 26: 17-23.

Physical Geography. 1898. p. 338.

Fairchild, H.L. Glacial Geology of Western New York. Geol. Mag. Lond.
HeGvemeile S. Cec. 4.9 41532.

Glacial’ Geology in America. Am. Ass’n Adv. Sci: Proc. 1898. 47:

27 -goam. Geol, 1898. 22: 154-89; Am. Sci. Sup. 1808. 0:
1183-85.

Elements of Geology. (LeConte) 1903. Paayly 57 Ts

New York drumlins (abstract). Geol. Soc. Am. Bul. Igo05. 16: 576.

——— Drumlin Structure and Origin. Geol. Soc. Am. Bul. 1907. 17: 702-7.

Geikie, James. Geol. Soc. Glasgow. Trans. 1867. 7
Whe Great Ice Age.” 1895. Ed. 3.
Chamberlin)

Earth Sculpture. 18098. - p. 234-35, 245, 378. — ;

Hall, James. Geol. N. Y.: Rep’t on Fourth District. 1843. p. 341, 414-15.

Hall, Six James. Roy. Soc. Edinburgh. Trans. 1815. 7: 169.

Harte, W. Roy. Geol. Soc. Ireland. Jour. , 1867.’ 2: 30.

Hitchcock, C. H. Lenticular Hills of Glacial Drift. Bost. Soc. Nat. Hist.
roc. 1879. 19: 63-67.

ientiewlar Halls. Am. Jour. Sct. 1884. Ill. 27: 72,

Johnson, Laurence. Parallel Drift Hills. of Western New York. N. Y.

Acad. Sci. An. 1883. 2:249-66, pl. 18. N. Y. Acad. Sci. Trans.
1882. 1: 78-80. :

Kinahan, G. H. & Close, H. M. General Glaciation of Iar-Connaught and

its Neighborhood, in the Counties of Galway and Mayo. Map.
Dublin 1872. ;

Leverett, Frank. Illinois Glacial Lobe.
HS8G:.= P- 73, 135-

Glacial Formations and Drainage Features of the Erie and Ohio

28 its
P- 17; 98, 411, 432, 743-45. (1. C:

Use Ss Geol Sur Monocr. 938:

Basins. U.S. Geol. Sur. Monogr. 41. 1902. p. 691-93, pl. III.
mi ieuwncad. ci, oth, An. Rept. 1904. p. 102.
——— Drumlins in the Grand Traverse Region of Michigan. Geol. Soc.
Acme, Bul. FQO5. 167-577.

Lewis, H.C. Second Geol. Sur. Pa. Rep’t Z. 1884. p. 28,

38 NEW YORK STATE MUSEUM

Lincoln, D. F. Glaciation in the Finger Lakes Region of New York. Am,
Jour. Sci. 1892. III. 44: 290-301. |

N. Y¥. State Mus. Rep’t 48. 1894. 2: 69-71.

Marbut, C. F. & Woodworth, J.B. Clays about Boston. U.S. Geol. Sur.
17th An. Rep’t. 1896. p. 995-08. 5

Matthew, G. F. Geol. & Nat. Hist. Sur. Can. Rep’t of Prog. 1877-78°
p- 12-14 EE. : }

Russell, I. C. Jour. Geol. 1895. 3: 831.

Glaciers of North America. 1897. p. 24-28.

—- Geol. Sur. Mich. Igo04. p. 69-81.

— Drumlin of Michigan. Geol. Soc. Am. Bul. Ig07. 17: 707.

——— Drumlin Areas in Northern pebip an: Geol. Soc. Am. Bul. 1905.
16:577-78.

Salisbury, R. D. Geol. Sur. N. J. An. Rep’t 1891. p. 71-74.

Aim’, Geol. 1803.—" 12.7172:

— Geol. Soc. Am. Bul. 1893. 4:9.

— Glacial Geology. Geol. Sur. N. J. 1902. 5: 103.

—— & Chamberlin, EB. ©. Geology. 1906... 3: 360.

Shaler, N. S. Bost. Soc Nat-Hist) Proc.) 18680 10-27.

On the Parallel Ridges of Glacial Drift in Eastern Massachusetts.
Bost. Soc. Nat. Hist. Proc. 1871. 13: 196-204. ao
— & Davis, W. M. [Illustrations of the Earth’s Surface: Glaciers.

1881. 4: 60-63.
—— U.S. Geol. Sur. 7th An. Rep’t. 1886. p. 321-22.
—-— U.S. Geol. Sur. goth An. Rep’t. 1888. p. 550-51.
Stone, G. H. Bost. Soc. Nat. Hist. Proc. 1881. 20: 434; Port. Soc. Nat.»
Hist, Proce. 188ae0 Mar Nove 2m.
Tarr, R.S. Origin of Drumlins. Am. Geol. 1894. 13: 393-407.
Physical Geography of New York State. Ig02. p. 144-51.

—— New Physical Geography. 1904. p. 152-53.
Taylor, Frank B. Distribution of. Drumlins and its Bearing on their
Origin. “Geol? Soc. Ant. Bul. 10077, 1 7e 726:

Tyrrell, J. B. Geol. Sur. Can:, An. Rep’t. 1888-89. n.s. 4:22 A.

———-— Geol; Sec. Amt bul) aSqo.8 71-402.

—— Geol. Sur. Can. 1892. * 6:15 A.

— — Am. Geol. 18093. I1: 132, 175.

Upham, Warren. Geology of New Hampshire. 1878. 3: 285-309.

——-— Glacial Deposits in New England.- Am. Ass’n Ady. Sci. Proc. 1879.

28: 309-10.
——— Glacial Drift in Boston and Vicinity. Bost. Soc. Nat. ce Proc:
1879. 20: 220-34.

—w— Marine Shells and Fragments of Shells in the Till near Boston.
Bost. Soc. Nat. Hist. Proc. 1888. 24:127-41; Am. Jour. Sci. 1889.
ser. 3. 37: 359-72.

Structure of Drumlins. Bost.Soc. Nat. Hist. Proc. 1889. 24: 228-42.

DRUMLINS OF CENTRAL WESTERN NEW YORK 430

— — Inequality of Distribution of the Englacial Drift. Geol. Soc. Am,
Bul. 1891. 3: 134-48.

——— Criteria of Englacial and Subglacial Drift. Am. Geol. 1891. 3:

; 376-85.

—— Conditions of Accumulations of Drumlins. Am. Geol. 1892.
IO; 339-62.

——— Geol. Soc. Am. Bul. 1892. 3: 140.

——— Origin of Drumlins. Bost. Soc. Nat. Hist. Proc. 1893. 202217.

——— Madison Type of Drumlins. Am. Geol. 1894. 14: 69-83.

——— Drumlin Accumulation. Am. Geol. 1895. 15: 194-95.

—— Drumlins and Marginal Moraines of Ice Sheets. Geol. Soc. Am. Bul.
BOQ. 7217-30. :

——— Drumlins Contained or Lying on Modified Drifts. Am. Geol. 1897.

20: 383-87.
Valley Moraines and Drumlins in the English Lake District. Am.
Geol. 1898. 21: 165-70.

——— Drumlinsin Glasgow. Am. Geol. 1898. 21: 235-43.

WreroG Gat. = Bost. Soc, Nat. Hist: Proc... 1876.- 19:58.

Bosmucocs, Nat. Elist:; Proc, 1881. 20: 217.

ammmmmncoe se 10 North America, Ed.4.- 1891.: p. 251-67.

——— Man and the Glacial Period. 1893. p. 75.

2

INDEX

Albion sheet, 306.

Areal distribution, 394-99.
Athabasca, drumlins, 394.
Attica-Geneva series, 398.

Barton, George H., cited, 3094, 406,
436.

Bibliography, 436-39.

Blind Bay bluff, 418.

Bonney, T. G., cited, 436.

Brockport sheet, 396.

Camillus shales, 414.

Canada, drumlins, 394.

Canastota, Salina shales, 396.
Cazenovia lake, drumlins, 390.
Chalmers, Robert, cited, 436.
Chamberlin, T. C., cited, 392, 304, 436.
Channels among drumlins, 427-29.
- Chautauqua lake, drumlins, 399.
Cline’s bluff, 418.

Clinton shale, thickness, 404.
Close, H. M., cited, 392, 435, 437.
Clyde sheet, 306, 426.

Cobleskill limestone, thickness, 404.
Concentric bedding, 416-19.
Connecticut, drumlins, 394.

Dana, J. D., cited, 437.

Dana, Lake, 306.

DWaxisee vy. I, cited, 302, 436, 437,

438. :

Dolphin back shape drumlins, 407.

Dome-shaped drumlins, 407.

Double-deck drumlins, 400.

Drift, in drumlin mass, 412; held in

the ice, factors relating to, 421.

Drumlinized drift, 303.

Drumlins, age, 429; altitude and
hight, 411; areal distribution, 394-
99; area, amount of land surface
included in, 399; bibliography, 436-
30; change to drift, 399; change to
moraines, 309; channels among,
427-29; composition and structure,

441

412-19; concentric bedding, 416-10;
definition, 392-93; depth of the
drumlin-making = ice, 434; district
of no elevated, 403; double-deck,
409; dynamic factors pertaining to
the ice body, 420-21; dynamics,
432-33; factors of external control,
422; factors relating to the drift
held in the ice, 421; formation,
theoretical mechanics, 419-20; form
and dimensions, 405-12; forms, 392,
433-34; forms and observed rela-
tions, 422-24; highland, 403; hight,
398, 300, 410; history of earlier
study, 392; internal structure, 413,
416; of Ireland, 392, 394, 435-36;
length, 412; most massive develop-
ment, 403; name first applied, 392;
former names, 392; name can not
be applied to ice-shaped rock
masses, 393; New York drumlin
area, 395; number in New York,
395; orientation, 399-402; origin,
431-32; constructional origin, 420;
product of continental glaciers, 391;
production or nonproduction, de-
pends on movement of bottom ice,
403; relation to larger topography,
402-4; relation to moraines, 424-
25; relation to underlying rock
strata, 404-5; secondary or contra-
wise forms, 402; may be partly
shale, 414; size and dimensions,
ANOe = SPeciali = teallukes, -94125—26 ;
thrust motion of the ground con-~
tact ice, 429-31; topographic ex-
pression, 393; abrupt ending of
topography, 399; wave cutting, 409.
Drumloid, term, 393.
Dynamics, 432-33.

England, drumlins, 394.

Fairchild, Efe lee ciredse 437:
Fairhaven, 397.

442 NEW YORK STATE MUSEUM

Fayetteville, Salina shales, 396.
Finger lakes series, western, 398.
Fulton, 397.

Ganargua creek, 428.

Geikie, James, cited, 392, 394, 437.
Genesee valley, 398.

Germany, drumlins, 394.

Hall, James, cited, 437.

fall, Sir James; cited, 302,437.
Hamilton shale, thickness, "404.
Harte, W., cited, 437. :
Hartnagel, C. A., cited, 404.
Hitcheock,-C. a. veited, so24437-

Ice body, dynamic factors pertaining
tO3A2Z0-2i-

Ireland, drumlins, 392, 3904, 435-30.

Iroquois, Lake, 396, 397.

J ohnson, Laurence, cited, 392, 437.

Keilhack, K., cited, 394.
Kinahan, G.-.7 cited, 02,435, 437.

Lake bluff, 418.

Leverett, Frank, cited, 437.
Lewis, H. C., cited, 437.

Lincoln, D. F., cited, 408, 438.
Lockport limestone, thickness, 404.
Lorraine shale, thickness, 404.

Macedon sheet, 428.

Mammillary form of drumlins, 407.

Manitoba, drumlins, 394.

Manlius limestone, thickness, 404.

Marbut, ©. Fs cited, 438:

Marcellus shale, thickness, 404.

Massachusetts, drumlins, 304.

Matthew, G. F., cited, 392, 304, 438.

Medina shale, thickness, 404.

Medina sheet, 306.

Mexico, 397.

Michigan area, 394.

Montezuma island groups, 426.

Moraines, change to drumlins, 390;
relation to drumlins, 424-25,

New England, area, 394. .

New York rocks along the Cayuga
meridian, 404-5.

Niagara-Genesee prairie, 396, 308.

Nondrumlin areas, 426-27.

Nova Scotia, drumlins, 394.

Oakfield-Syracuse series,
ANC Oa eS
Oneida, Salina shales, 396.

-Onondaga limestone, thickness, 404.

Ontario drumlin area, 395.

Ontario series, eastern, 398, 400.
Orientation, 399-402.

Oriskany sandstone, thickness, 404.
Oswego sandstone, thickness, 404.
Oswego sheet, 418.

Oval form drumlins, 407.

Palmyra sheet, 395, 306, 428.
Pulaski drumlins, 397, 400-1.

. Pulaski sheet, 395.

Pultneyville sheet, 418.

Ridge form drumlins, 407.

Ridge road, 307. |

Rocdrumlins, 393, 395, 413-16, 431.

Rocdrumloid, 393.

Rochester shale, (ificlaeess 404.

Rock strata, underlying, relation of
drumlins to, 404-5.

Rondout waterlime, thickness, 404.

Russell, I. C., cited, 438.

Sacketts Harbor sheet, 395.

Salina shale, 413, 416; thickness, 404,
Salisbury, R. D., cited, 438. -

Sand in drumlin mass, 413.
Scandinavia, drumlins, 394.
Scotland, drumlins, 394:

Seneca river, 428.

Shale hills, see Rocdrumlins.

Shale in drumlin mass, 414.

Shaler, N. S., cited; 302,437, 420:
Sodus, 397.

Sodus bay sheet, 418.

Stone, G. H., cited, 438.

Sweden, drumlins, 304.

Switzerland, drumlins, 394.

Syracuse drumlin area, 396, 307, 403.

opti

—

[

i

h

i} > : E

,

INDEX TO DRUMLINS OF CENTRAL WESTERN NEW YORK 443

Syracuse island masses, 425-26. Utica shale, thickness, 404.

Syracuse sheet, 428.
; Vernon shales, 413, 414, 431.

‘Tarr, R. S., cited, 438.

Taylor, Frank B., cited, 424, 438. Warren, Lake, 306.
Thrust motion of the ground contact | Watertown sheet, 305.

ice, 429-31. Wave cutting of drumlins, 4009.
Till, drumlins composed of, 412. Weedsport sheet, 396, 428.
Tyrrell, J. B., cited, 394, 438. Wisconsin, drumlins, 394.

. Woodworth, J. B., cited, 438.
Upham, Warren, cited, 392, 304, 416, | Wright, G. F., cited, 439.
436, 438-39.

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New York State Education Department
New York State Museum
/ JOHN M. CrarKkeE, Director

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G4 (48) Woodworth, J. B. Pleistocene Geology of Nassau County and
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Gs (56) Merrill, F. J. H. Description of the State feseliog | Map of igor.
42p. 2 inaps, tab: | Oct. 1902)" 168.
G6 (77) Cushing, H. P. Geology of the Vicinity of Little Falls, Herkimer
Co. 98p: il. tspl. 2 maps) S]an. T9O5-) =3oG
G7 (83) code ced J.B. Pleistocene Geology of thie Mooers Quadrangle.
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G8 (84) Ancient Water Bs of the Champlain and Hudson Valieys.
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Gg (95) Cushing, H. P. Geology of the Northern Adirondack Region.
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Gio (96) Ogilvie, I. H. eoleay of the Paradox Lake Quadrangle. 54p.
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Gi2 aon Wocduers eR ae Papen C. A.: Whitlock, H. P.; Hudson,
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388p. ‘s6pl. map. May T9074) OCC, ‘cloth.
Contents: Woodworth J. B. Postglacial Faults of Eastern New York.
Hartnagel, C. A. Stratigraphic Relations of the Oneida Conglomerate.
—— Upper Siluric and Lower Devonic Formations of the Skunnemunk Mountain Region.
Whitlock, H. P. Minerals from Lyon Mountain, Clinton Co. y
Hudson, G. H. On Some Pelmatozoa from the Chazy Limestone of New York. i
Clarke, 1p M. Some New Devonic Fossils. :
eee Interesting Style of Sand-filled Vein. 4
—— Eurypterus Shales of the Shawangunk Mountains in Eastern New York. a
White, David. A Remarkable Fossil Tree Trunk from the Middle Devonic of New York. 4
Berkey, ee P. Structural and Stratigraphic Features of the Basal Gneisses of the
ighlands.

G13 (111) Fairchild, H. L. Drumlins of New York. 58p. 28pl. 19 maps.
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Later Glacial Waters j in Central New York. Prepared.

Cushing, H. P. Geology of the Theresa Quadrangle. In preparation.

Geology of the Long Lake Quadrangle. In press.

Berkey, C. P. Geology of the Highlands of the Hudson. In preparation.

Economic geology. Egr (3) Smock, J. C. Building Stone in the State of
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Eg2 (7) First Report on the Iron Mines and Iron Ore Dictricts in
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Ee eT a

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M2 (58) Whitlock, H. P. Guide to the Mineralogic Collections of the New

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M3 (70) —— New York Mineral Localities. a11op. Sep. 1903. 2006.

M4 (98) —— Contributions from the Mineralogic Laboratory. 38p. 7pl.
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Pa2 (30) Clarke, J. M.; Simpson, G. B. & Loomis, F. B, Paleontologic
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Contents: Clarke, J. M. A Remarkable Occurrence of Orthoceras in the Oneonta Beds of

the Chenango Valley, N. Y.
—— Paropsonema cryptophya; a Peculiar Echinoderm from the Intumescens-zone

(Portage Beds) of Western New York.
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—— The Water Biscuit of Squaw Island, Canandaigua Lake, N. Y.
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Wood, Elvira. Marcellus Limestones of Lancaster, Erie Co. N. Y.
Clarke, J: M. New Agelacrinites.
—— Value of Amnigenia as an Indicator of Fresh-water Deposits during the Devonic of

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Pa6 (52) Clarke, J. M. Report of the State Paleontologist root. 28op. il.

opl. map, 1 tab. july en9o2. AGc.

_ Pay (63) —— Stratigraphy of Canandaigua and Naples Quadrangles.

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_ White, David. The Devonic:Plants of New York. In preparation.

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Hudson, G. H. Geology of Valcour Island. In preparation.

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Report of the State Paleontologist 1902. 464p. 52pl. 8 maps.

~

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En7 (26) - Collection, Preservation and Distribution of New York In-
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Bo3 (25) - Report of the State Botanist 1898. 76p. 5pl. Oct. 1899.
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Museum memoirs 1889-—date. :

t Beecher, C. E. & Clarke, J. M. Development of Some Silurian Brachi-
op oda. oop. Sply “Oct 1889. ob 5,

2 Hall, James & Clarke, J. M. Paleozoic Reticulate Sponges. 35o0p. il. 7opl.
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3 Clarke, J. M. The Oriskany Fauna of Becraft Mountain, Columbia Co.
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6 ees M. Naples Fauna in Western New York. 268p. 26pl. map.

2, ctoth.

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220). rspl. 1907. $1.25 ctoth. o
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Natural history of New York. 3ov. il. pl. maps. Q. ieee 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- — Es]
ate illustrations. 5v.il.pl. maps. sq.Q. Albany 1842-44. Out of print. a
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v. 1 ptr Mammalia. 1314+46p. 33pl. 1842. 4
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DIVISION 2 BOTANY. Torrey, John. Flora of the State of (New York: com-
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properties. av. il. pl. sq Q. Albany 1843. Out of print.

v. t Flora of the State Ls New York. © 12 +484p. 72pl. 1843.

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v. 2 Flora of the State of New York. 572p. 89pl. 1843.
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DIVISION’ 3 MINERALOGY. Beck, Lewis C. Mineralogy of New York; com-
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‘of New York, and notices of their uses in the arts and agriculture. il. pl.
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Vin iE ptr Economical Mineralogy. pt2 Bee cripale Mineralogy. 24+5306p.
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. 8 plates additional to those printed as ait of the text.

DIVISION 4 GEOLOGY. Mather, W. W.; Emmons, Ebenezer; Vanuxem, Lard-.
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1842-43. Out of print.

v. t ptr Mather, W. W. First Geological District. 37+6s53p. 46pl. 1843.

v. 2 pt2e Emmons, Ebenezer. Second Geological District. 10+437p. 17pl.

/ 1842.

Vv. 3 pt3 Vanuxem, abaedvier. Third Geological District. 306p. 1842.

We (44 pta.*Fall; James. Fourth Geological District. 22+683p. t1o9pl. map.
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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-
ee productions of the State. sv. il. pl. sq.Q. Albany 1846-54. Out
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Wee oils of the State, their Composition and Distribution. 11 +371p. 2rpl.
18406.

v. 2 Analysis of Soils, Plants, Cereals, etc. 8 +343 +46p. 42pl. 1849.
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Tease Hives, ete:- 8+340p. 18511,

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DIVISION 6 PALEONTOLOGY. Hall, James. Palaeontology of New York. 8v.
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v. 1 Organic Remains of the Lower Division of the New York System.
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Vv. 3 Organic Remains of the Lower Helderberg Group and the Oriskany
Peoandcteme. pti, text. .12-+532p: .1859.- [$3.50] ;
(2. wagpl. .1867. [oe 50|
4 Fossil Brachiopoda of the Upper Helderberg, Hamilton, Poni and
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Weg ptr Lamellibranchiata t. Monomyaria of the Upper Helderberg,
Hamilton. and Chemung Groups. 18+268p. 45pl. 1884. , $2.50.
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pte Gasteropoda, Pteropoda and Cephalopoda of the Upper Helder-
berg, Hamilton, Portage and Chemung Groups. 2v. 1879. v. 1, text.
Meee V2, t20pli .$2.50-for 2-9:
—— & Simpson, George Bi} v0 Cosals and biyozoa of the Lower and Up-
per Helderberg and Hamilton Groups. 24+208p. 67pl. 1887.. $2.50.
& Clarke, John M. v. 7 Trilobites and other Crustacea of the Oris-
kany, Upper Helderberg, Hamilton, Portage, Chemung and Catskill
Craups. (64--236p. 4opl. 1888." Cont. supplement to v. 5, ptz. Pterop-
oda, Cephalopoda and ooo Age Spl, “18Ssi9 £2 ov;

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& Clarke, John M. v. 8 ptr Introduction to the Study of the Genera’

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

& Clarke, John M. v. 8 pt2 Paleozoic Brachiopoda. 16+394p. 64pl.
_ 1894. ‘epa O

Catalogue of the, Cabinet of Natural History of the State of New York and
a the Historical and Antiquarian Collection eee OL thereto, 44ap.450)

853.
He ndvuas 1893—date. bite
In quantities, 1 cent for each 16 pages orless. Single copies postpaid as below.
. New York State Museum. s52p.il. 4c. .
Outlines history and work of the museum with list of staff r902.

Paleontology. t12p. 2c¢.

Brief outline of State Museum work in paleontology under heads: Definition; Relation to

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Guide to Excursions in the Fossiliferous Rocks of New York. 124p. 8c.

Itineraries of 32 trips covering nearly the entire series of Paleozoic rocks, prepared specially |

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Entomology. 16p. 2c.

Economic Geology. 44p. 4c.

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Classification of New York Series of Geologic Formations. 321... BG:

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, Vv: 1... 59K67.em. 18094. .Scale 14 miles to 1 imch: ¥25e:

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. ty, T8O7. PoC.

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
Sullivan, Ulster and Suffolk counties; also northeastern New Jersey and part of western

onnecticut.

Map of New York Showing the Surface Configuration and Water Sheds.

1901, Scale 12 milesto rinch. J5c.

Map of the State of New York Showing the Location of its Economic
Deposits. 1904. Scale 12 miles to 1 inch. 5c.

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

*Albany county. Mus. rep’t 49, v. 2. 1898. 50c.

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

Vicinity of Frankfort Hill [parts of Herkimer and — counties]. Mus.
Ep t i5\l, Vie. TOOO.

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

Amsterdam quadrangle. Mus. bul. 34. 1900.

*Parts of Albany and Rensselaer counties. Mus. bul. 42. 1901. 0c.

*Niagara. river...Mus,-bul. 45. .1901. 25¢.

Part of Clinton county. State geol. rep’t 19. rgo01.

Oyster Bay and Hempstead quadrangles on Long Island. Mus. bul. i
IQOTI.

Be icas of Clinton and Essex counties. Mus. bul. 52. 1902.

Part of town of Northumberland, Saratoga co. State geol. rep’t 21. 1903.

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

*Olean quadrangle. Mus. bul. 69. 1903. 0c.

*Becraft Mt with. 2 sheets of sections. (Scale 1 in. = 4 m.) Mus. bul. "s
FOR. |. 206.

*Canandaigua-Naples quadrangles. Mus. bul. 6 3. 1904. 20c.

*Little Falls quadrangle. Mus. bul. 77. 1905. dc.

*Watkins-Elmira quadrangles. Mus. bul. 81. 1905. 20c¢.

*Tully quadrangle. Mus. bul. 82. 1903. 0c.

*Salamanca quadrangle. Mus. bul. 80. 10905. ° 0c

*Buffalo quadrangle. Mus. bul. 99. 1906. J0c. :

*Penn Yan-Hammondsport quadrangles. Mus. bul. ror. 1906. 20¢.

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