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Published monthly by the
Shea York State Education Department*
: peeeareaN ge JANUARY 1908
“ is. § Si ie 2 ‘
Ne ew v York State Museum
Joun M. Crarke, Director
Bulletin 118
PALEONTOLOGY 18
_ SEoLoGIC MAP AND DESCRIPTIONS
ae
* *
4 ni ; OF}. THE
"PORTAGE AND NUNDA QUADRANGLES
4 Bh “INCLUDING A MAP OF LETCHWORTH PARK
r 5 Ses i } ; BY
Bae JOHN M. CLARKE & D. DANA LUTHER
ACCOMPANIED BY A REPORT ON THE
'
7 — (
PLEISTOCENE HISTORY OF THE
So. | GENESEE VALLEY
3 : | BY ‘
Ses | HERMAN L. FAIRCHILD
4 i ; . PAGE _. PAGE
Geology of the Povedge and Evolution of western New
-Nunda Quadrangles. J. M. . York \dtainage:s: «iia teane 70
~Crarke & D. D. LUTHER. 43; “Diverstans “ef, the “river.
Bee duction POR doa SNe 14S Burted vehatinels:..)..... <r 71
PeieiSrical Sie eee % ... 44] Glacial waters and canyon
Piptiegraphy........ Shee oh Menthe: .: <p een cms « 75
init RVGSEIRCAUON. vo .ic cess + 46 Pater stames ioe. cs. edad 81
See Description of formations... 47 Epitome of the history..... 81
a Be eh Co ay, Oe ar 68 | Canyons and cataracts..... 81
ke Pleistocene History of the | Deformation of the lake
Bn ts Genesee Valley in the PME ie ee ee? 83
See SP ortace: District. HA. L. Detrital filling of the valleys 84.
LRU Sie, ens 9 ao eR ETM ERY AWS ay Shay lv Wack bie lide 4 hm 85
ALBANY
NEW YORK STATE EDUCATION DEPARTMENT
1908 ©
Ppipe 35 cents
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nee ee
_ STATE OF NEW YORK
EDUCATION DEPARTMENT © Sa
Regents of the University |
_ With years when terms ee 3 3
1913. WHITELAW Rew M.A: LL.D.D.C.L. Chancellor New York 3
1917 St Cram McKetway M.A. LL.D. Vice Chancellor Brooklyn |
[oes DANIEL Beacn Ph.D: LL.D...” ..°« . “= =9 Va ‘
pigi4-Peiny-T. Sexton LL.B. LUD... . 2) 2a
Sror2 1. Guitrorp Smirh M.A. C.E. LL.D. °.°>, “Bufaia .
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1915 ALBERT VANDER VEER M.D. M.A. Ph.D. LL.D. . Albany
1911 Epwarp LAuTERBACH M.A. LL.D. . « 5 New
isco. GENE A. Pai.sin. LLB: LL.DD 2 = 2S New York
so10 Lucian L. SHeppen LL.B. .. .. . .. .. Platteeee
Commissioner of Education
ANDREW S. Draper LL.B. LL.D.
Assistant Commissioners a
_ Howarp J. Rocers M.A. LL.D. First Assistant
-Epwarp J. Goopwin Lit.D, L.H.D. Second Assistant
Aucustus S. Downinc M.A. Pd.D. LL.D. Third Assistant —
Director of State Library
Epwin H. AnpeErRsSoN M.A.
Director of Science and State Museum
Joun M. Crarxke Ph.D. LL.D.
-
Chiefs of Divisions
- Administration, HarLan H. Horner ‘B.A.
Attendance, JAMES D. SULLIVAN
Educational Extension, WILLIAM R. EASTMAN M.A. M.L.S.
Examinations, CHARLES F. WHEELOCK B.S. LL.D.
Inspections, FranK H. Woop M.A.
Law, THomas E. FINEGAN M.A.
School Libraries, CHARLES E. Fitcu L. H. D.
Statistics, Hiram C. Case
~ Visual Instruction, DELANcey M. Ettis
New York State Education Depariment
Science Division, March 7, 1907
Hon, Andrew S. Draper LL.D.
Commissioner of Education
My bear sir: I communicate herewith, for publication as a
bulletin of the State Museum, geological maps on the scale of
1 mile to 1 inch, of the Nunda and Portage quadrangles, accom-
panied by a description of the geological structure of these regions
an including also a map of Letchworth Park with its geology and
a report on the Pleistocene History of the Genesee Valley in the
Portage District.
Very respectfully yours
Joun M. CLARKE
Director
State of New York
Education Department
COMMISSIONER'S ROOM
Approved for publication this oth day of March 1907
AS Ribera
Commissioner of Education
New York State Education Department
New York State Museum
JoHN M. Crarke, Director
Bulletin 118
PALEONTOLOGY 18
GEOLOGIC MAP AND DESCRIPTIONS OF THE
_ PORTAGE AND NUNDA QUADRANGLES
_ INCLUDING A MAP OF LETCHWORTH PARK
BY
JOHN M. CLARKE AND D. DANA LUTHER
ACCOMPANIED BY A REPORT ON THE
PLEISTOCENE HISTORY OF THE GENESEE VALLEY
| BY
' HERMAN L. FAIRCHILD
GEOLOGY OF THE PORTAGE AND NUNDA
QUADRANGLES
INTRODUCTION
The region whose geological structure is here described in detail
is not alone celebrated in the history of New York geology for the
completeness of its presentments, the uniformity of its strati-
graphy and the fullness of its ancient faunas, but its human
history is romantic and its scenic features singularly attractive.
The Nunda and Portage quadrangles cover a territory 17 miles
long from north to south and 26 miles wide, through which
in winding course runs the great gorge of the Genesee river,
extending from Portage down to Mount Morris, a distance of 18
44 NEW YORK STATE MUSEUM
miles by the stream. Along the vertical walls of the canyon the
cliffs rise from 200 to 350 feet displaying the even, regular beds
of the rock formations so elaborately and lucidly as to invite the
attention of the geological student, while all the attendant phe-
nomena of the erosion of the gorge and the history of this great
drainage way throughout its many vacillations afford subjects of
added interest. The Genesee river crossing the entire State from
north to south is the line of most continuous meridional section
through the geological formations of western New York. Very
naturally then, when the Geological Survey of New York was
organized (1836) and the fourth or western district erected (1837),
the rock exposures of this stream invited immediate attention. Not
only has this trunk stream cut deep into the rock strata but its
contributories, Cashaqua creek, Wolf creek, Buck run, Silver lake
inlet and Wiscoy creek add other means of completing the details
of geological structure so that data are not lacking on every hand
to solve the problems of geological history. Public attention and
interest has been recently drawn to this region by the erection
within its boundaries of a new public preserve — Letchworth Park
—the beneficent gift to the people of the State of New York by
the Hon. William Pryor Letchworth, to whose munificence and
long public service the place will be a perpetual monument: This
beautiful property embraces the three cataracts of the Genesee
river and the banks adjoining. It is with some satisfaction that,
with the aid of Mr Letchworth, we are enabled here to present
a special map of this park with its geology given in detail.
HISTORICAL
Bibliography
The rocks and fossils of this portion of the Genesee river section
have been the subject of, or have contributed freely to many of
the publications of the New York survey. It is not the purpose
here to review these in detail as this publication is chiefly designed
to explain the accompanying maps. Students will find more or —
less adequate accounts of the geology and paleontology of the
formations involved in the works here cited. i
1 The original and fundamental documents upon the region are
the Second and Fourth Annual Reports (1836, 1838) and the
final report of the geologist in charge of the fourth geological
district (1843), James Hall. |
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PORTAGE AND NUNDA QUADRANGLES 45
‘The first of these was accompanied by a perspective map (here
reproduced) of the Genesee river prepared by Eben N. Horsford,
assistant to Professor Hall and then a resident of Moscow.!
2 Palaeontology of New York, v. 5, 6, 8.
In these volumes are descriptions of many of the fossils occur-
ring in the rocks of these quadrangles.
3 The Higher Devonian Faunas of Ontario County, N. Y. John
MerClarke. U.S. Geol. Sur. Bul. 16... 1885.
Though chiefly concerned with the stratigraphy and paleontology
in a section further to the east this treatise applies to and in con-
siderable measure was based upon the Portage group of the Genesee
miver. |
4 Faunas of the Upper Devonian, Genesee Section of New York.
fPessevvilkiams. WU. S. Geol: Sur. Bul. 41. 1888:
5 stratigraphic Value of the Portage Sandstones. D. D. Luther.
ieee tate Mus. Bul. 52.1902. p: 616-32.
Traces the upper sandstones of the Upper Falls at Portage east-
ward and shows their continuity with the High Point sandstones
of Ontario county. In the same paper J. M. Clarke shows that
the fauna of this sedimentation unit is entirely different at the
east from that in the Genesee valley, at the former containing a
Chemung brachiopod assemblage, in the latter the typical Portage
fauna with cephalopods and lamellibranchs.
6 Geologic conditions at the Site of the Proposed Dam and Stor-
age Reservoir on the Genesee River at Portage. John M.
Clarke. An. Rep’t State Engineer and Surveyor for 1896, p.
106-22.
7 Naples Fauna in Western New York. John M. Clarke. pt I.
mee state Geol. 16th An. Rep’t.. 1898; pt 2. N. Y. State
Mus. Mem. 6. 1903. 3
This work describes and illustrates the fauna of the Portage
group in its entirety, discusses its bionomic relations and elucidates
‘the stratigraphy of the formation.
8 Stratigraphy of the Portage Formation between the Genesee
Valley and Lake Erie. D. D..Luther. N. Y. State Mus. Bul.
: 69. 1903. p. 1000-20.
————
_ *Mr Horsford, after serving as a teacher at Geneseo and at Albany,
became the distinguished Rumford professor of chemistry at Harvard Uni-
versity. The rocks and fossils of the Genesee valley have inspired other
men to distinction. Maj. John W. Powell, late director of the United
States Geological Survey was a native of Mount Morris, and the eminent
paleontologist Prof. O. C. Marsh was born on the richly fossiliferous rocks
Grossing the lower Genesee and not far from its western boundary,
t
:
46 NEW YORK STATE MUSEUM
Classification
The rock strata of the Genesee river section have been broadly
classified and generally known under the names “ Genesee,” for
the black shale at the mouth of the gorge, ‘‘ Portage ” for the shales
and sandstones displayed above in the walls of the gorge, and
“ Chemung” for the sandstones and shales exposed in the ravines
and along the river bed south of Portage to the State line, names
applied at the time of the first geological survey of the State, 1837
to 1843.
In this bulletin the ‘precise and detailed classification of these
rocks defines more exactly the significance of each of these appella-
tions, as explained under the appropriate titles. Of most com-
manding importance in the rock succession of this region is the
series of strata historically known as the “ Portage Group.” To
validate the integrity of this term against incursion its origin baat
purpose are ma briefly recalled.
The name “ Portage’”’ was first used in connection with the geo-
logical series of the State by James Hall in 1840 (Fourth Annual
Report on the Fourth Geological District), when describing with
some detail the rock section exposed in the Genesee River gorge
between Mount Morris and Portageville. The following divisions
were made: Cashaqua shale, Gardeau or Lower Fucoidal group
and Portage or Upper Fucoidal group.
The last division included the strata between the Table rock at
the top of the Lower Portage falls and the top of the heavy sand-
stones above the Upper falls, an aggregate of 425 feet of which
210 feet are shales and flags, not essentially different either in
lithology or fossils from the beds below the Table rock and included
in the Gardeau group, except as to the presence in the upper of
Fucoides verticalis.
In 1843 (Final Report on the Geology of the Fourth District,
page 224), Professor Hall dropped the terms “ Upper Fucoidal ”
and “Lower Fucoidal,’ and the expression “ Portage or Nunda
group” is employed to include “ Cashaqua shale,” “ Gardeau shale
and flags” and “ Portage sandstones,’ no change being made in
the descriptions of these members of the Portage group..
It thus appears that the word “Portage” was first used as a
group term, not as the description of a member of a group or unit.
It was so employed by Hall in all subsequent writings.
PORTAGE AND NUNDA QUADRANGLES 47
The introduction of the name “ Nunda” as an alternative term
was unfortunate and is not now easily explainable, as the town
of Portage was set off from the town of Nunda, March 8, 1827,
and the new town included all of the territory along the banks of
the Genesee river previously lying in the town of Nunda; but in
April 1846, that part of Portage township on the west side of the
river with a strip taken from the town of Pike, was erected into a
new town and named Genesee Falls.
Of the units composing the Portage group, the Cashaqua shale
is not exposed at all within the present limits of the township of
Nunda, and the Gardeau shale and flags as delimited by Hall appear
in but a few small isolated exposures, the heavy sandstones (Port-
age sandstones) at the top being the only part of the group that
can be said to be fairly well exposed in the town and only to these
can the name Nunda with any propriety be applied.
The term “ Portage group” has been in use for more than 60
years by students of geology and has acquired recognition by the
general public as the designation of the strata between the Genesee
black slate and the Chemung sandstones. Historically, logically and
legitimately it is substantially fixed.
Exhaustive studies of the stratigraphy and paleontology of the
rock section in the Genesee gorge have shown that Table rock at
the top of the Lower falls, differs from other sandstones above and
below it only by being slightly harder and more calcareous, and by
a more abrupt transition to soft shale in the upper surface, the sedi-
mentation above it up to nearly the top of the Upper falls being of
the same character as the beds below it down to the mouth of Wolf
creek; the same fossils occur above and below it. Therefore recent
publications by this department have fixed the upper limit of the
Gardeau flags at the base of the heavy sandstones near the top of
the Upper falls.
To avoid the confusion by duplication of the original group term
“Portage ” with the later unit term ‘‘ Portage sandstones,” we shall
here substitute for the latter the term “ Nunda sandstone” as the
designation for the upper terminal member of the Portage group as
Hall defined it.
Description of formations
All the geologic formations represented on the area here con-
sidered belong to the upper division of the Devonic system,
48 NEW YORK STATE MUSEUM
The following is the succession in descending order and the
formations are considered in order from bottom to top.
f Upper 1 4251
Chemung sandstones
Chautauquan \ and Shales
Lower | ) =
Wiscoy shale _ 190°
Nunda sandstone | 215)
.|Gardeau flags and shale ~ 3441
Neodevonic Grimes sandstone | gs
Hatch flags and shale 2041
Ganeeae Rhinestreet black shale 53)
Cashaqua shale 125!
Middlesex black shale set
West River black shale 65?
Genundewa limestone 8
Genesee black shale 5}
The aggregate thickness of the beds here described is 2142 feet.
The difference in altitude between the Genesee river bed at the
north line of the Nunda quadrangle and the highest point near the —
southwest corner of the Portage quadrangle is 1565 feet and 578
feet additional are brought up by the elevation of the strata towa.d
the north and east.
Genesee shale
The lowest rock exposure on this area is the Genesee black shale.
Historical. This formation was first described in the 3d Annual
Report by Hall, 1839, page 301, under the title ‘‘ Upper black shale,”
beginning, “ Reposing upon the Tully limestone we have a thickness
of 150 feet of shale exhibiting throughout a uniform color, and
slaty structure” etc.
The black shale is mentioned several times in this report, as
occurring in Seneca, Yates and Ontario counties, but no more
specific name is applied to it. It is also referred to in the 4th
Annual Report.
In the final report of 1843, page “ie the name Genesee slate is
substituted for Upper black shale, and the opening of the gorge of
the Genesee river at Mount Morris is said to be the place of its
greatest development in the district.
PORTAGE AND NUNDA QUADRANGLES 49
As usually described in the annual and final reports it immediately
overlies the Tully limestone or, when that is wanting, the Moscow
shale, and is succeeded by the beds of greenish shale afterward
given the name Cashaqua shale, but on page 422 of the report for
1839, after mentioning the localities of several exposures of the
Upper black shale in the vicinity of Moscow and Geneseo, including
the one at Fall brook, where it is stated “ the water leaps a hundred
feet from the top of this rock,” Hall says: “In this neighborhood
the black shale is succeeded by a stratum of thin limestone.”
In the final report on the fourth geological district, page 227,
where describing the Cashaqua shale he says: “On tracing it (the
Cashaqua shale) west of the Genesee, it constantly presents the
same features as on the Cashaqua creek, though the lower part 1s
sometimes dark colored and separated from the Genesee slate by a
thin calcareous band,” evidently referring to the limestones at the
top of the falls at Fall brook and in the ravine of Little Beards
creek at Moscow which also appear in all exposures of this horizon
between Ontario county and Lake Erie, and are now known as the
Genundewa limestones, more fully described in the succeeding
pages. That it is the stratum referred to by Hall is made certain
by the fact that there is no other continuous limestone above it in
the Genesee river section, nor elsewhere in this State west of On-
tario county.
There are 83 feet of Genesee black shale between the horizon of
the Tully limestone and the Genundewa limestone at Fall brook and
too feet of dark and black shales between the Genundewa lime-
stone and the base of the Cashaqua shale at the mouth of the gorge.
The latter beds have been commonly known as Upper Genesee, but
the difference in the character of the shale above and below the
Genundewa limestone, and in their faunas, has made it proper, as
further explained in New York State Museum bulletin 63, page 25,
to restrict the use of the name “ Genesee ” to the beds between the
horizon of the Tully limestone and the Genundewa limestone.
As thus defined the only exposure of this formation on these
quadrangles is at the west end of the highway bridge over the
Genesee river at Mount Morris in the lower part of a small out-
crop on the north side of the bridge. At times of low water the
exposure is 15 to 20 feet long and 6 to 8 feet high.
The shale here is very dark, but somewhat more calcareous and
less bituminous than the beds below, which are, for the most part,
densely black and on exposure become very fissile and split into
50 NEW YORK STATE MUSEUM
large flat plates. Spherical concretions are common throughout
the Genesee shale.
Fossils are very rare in this formas specially in the more
bituminous beds. Drifted land plants and conodont teeth some-
times occur in the black shale, and the more calcareous layers to-
ward the top contain:
Pleurotomaria rugulata Hall Orbiculoidea lodensis (V anuxem)
Styliolina fissurella (Hall) Liorhynchus quadricostatus Hall
Pterochaenia fragilis (Hall) Probeloceras lutheri Clarke
Lingula spatuiata Hall Bactrites aciculum (Hall)
The entire section of the Genesee slate is well exposed in several
ravines north of Moscow and in the Fall brook ravine at Geneseo
below the top of the falls and in numerous other localities along
its line of outcrops, which extends from Chenango county to Lake
Erie.
Genundewa limestone
The stratum of impure limestone referred to by Hall as suc- :
ceeding the Genesee slate in the vicinity of Moscow and Geneseo, is
the heaviest of a series of similar character that seems to have
escaped farther notice until 1882, when it was described by Clarke,
in United States Geological Survey bulletin 16, as the “ ie aie
band.”
In New York State Museum memoir 6, N ae Fauna in West-
ern New York, pt 2, Clarke, 1903, and in Bulletin 63, Clarke and
Luther, 1904, it is more fully described as a unit of sedimentation in
the Genesee beds and designated Genundewa limestone on account
of its very favorable exposure at Genundewa Point on the east side
of Canandaigua lake.
This horizon is quite calcareous and concretionary as far east as
Cayuga lake, but the limestone first appears as distinct layers in
Gorham, Ontario co., when westward it is continuous to Lake Erie,
its peculiar structure making it easy of recognition wherever ex-
posed.
In the Genesee valley region it is composed of five layers of dark
gray bituminous limestone from 2 to 14 inches thick separated by
layers of dark shale from 1 to 6 inches thick. Some of the lime-
stones are even and flaggy, while others are concretionary and the
laminations of the intervening shale are bent to conform with their
very uneven surfaces.
The entire band was formerly exposed at the west end of the
Pennsylvania Railroad bridge over the river at Mount Morris,
: Plate I
View of lower part of the Genesee gorge from the High banks. Looking
toward the northeast. Rhinestreet black shale in front; lower part of cliff
in distance is Cashaqua shale
PORTAGE AND NUNDA QUADRANGLES 51
but since the erection of the dam below it only appears at the
west end of the highway bridge immediately north of the dam,
where the lower layers may be seen above the outcrop of black
Genesee slate previously mentioned.
Fossils are abundant and peculiar, the purer limestone being
composed almost wholly of the minute shells of the pteropod
miyliolina fissurella (Hall) and the entire fauna has
very close relations with that peculiar to the Portage beds above.
It is the earliest appearance in New York of the Naples fauna or
the world-wide zone of Manticoceras intumescens.
The following are common species, but for the full list with
descriptions and illustrations consult Naples Fauna in Western
New York, pt 1 and 2.
Manticoceras pattersoni (Hall) var. Honeoyea styliophila Clarke
styliophilum Clarke Buchiola retrostriata (v. Buch)
Gephyroceras genundewa Clarke Pterochaenia fragilis (Hall)
Tornoceras uniangulare (Conrad) Aulopora annectens Clarke
Phragmostoma natator Hail Melocrinus clarkei Williams
In the vicinity of these quadrangles favorable exposures of the
Genundewa limestone may be found in several ravines along the
west side of the Delaware, Lackawanna and Western Railroad
between Moscow and Greigsville, also at the top of the falls in the
Fall brook ravine at Geneseo and along the east and west road
34 miles south of the same falls.
It causes cascades in many ravines in Livingston and Ontario
counties and is well exposed in the bed of Murder creek at Gris-
wold, Wyoming co.
West River shale
A bed of dark to black shale about 100 feet thick succeeds the
Genundewa limestone in this section. The lower part is covered
by the water above the Mount Morris dam but the upper part is
finely exposed in the cliff on the east side of the mouth of the
gorge.
For about 62 feet next above the limestone the shales are mainly
‘dark gray or blue black with thin layers of densely black and slaty
bituminous shale 4 to 6 inches thick occurring at intervals of 2 to 6
feet, producing in this and other cliffs of these beds a distinct
banded effect.
These shales are contrasted with the Genesee shale below by
their generally lighter color and less bituminous character. They
are also more fossiliferous, though the number of species repre-
52 NEW YORK STATE MUSEUM
sented is but slightly increased by the addition of a few of the
forms that first appear in the Genundewa limestone.
The following are the more common fossils:
Bactrites aciculum (Hall) Buchiola retrostriata (v. Buch)
Pleurotomaria rugulata Hall Lingula spatulata Vanuxem
Pterochaenia fragilis (Hall) Orbiculoidea lodensis (Vanusem)
Spheric and oblong concretions occurring singly or in rows are
common and have been collected in many places on account of their
symmetry or their sometimes curious forms suggestive of “ petri-
fied turtles,” “ Indian skulls, stone hats,” “‘ stone ducks ”’ etc.
No exposure of these beds but the one at the mouth of the —
gorge, which is continuous up the river for about a mile, is found
on these quadrangles, but they may be seen to good advantage
above the falls in the Moscow ravine, 3 miles farther north and
in the upper part of the Fall brook gully. |
The name “ West River shales” was first applied to these beJs
above the Genundewa limestone by Clarke and Luther in Bulletin
63, 1904, on account of their abundant exposure in the ravines of
the West river valley in Yates county and to meet the require-
ments of a stratigraphic term for the residuary member of the old
Genesee division. .
99 66
Standish shale
At the top of the West River beds there are in this section a
few lighter colored layers, some clayey, others slightly arenaceous,
altogether about 3 feet in thickness.
This lighter band which has the lithic characters of the shales
and flags of the Portage group and contains a few fossils from
both the Genesee and Portage faunas, is hardly noticeable here, is
more fully developed in the Canandaigua lake valley and is known
as the Standish shales and flags. It is not represented in the
coloring on this map.
Middlesex shale
This passage bed is succeeded by 32 feet of densely blac
bituminous slaty shales that show a marked contrast to the
West River shales lithologically and in being almost entirely
barren of fossils except lignites, which are common, and a few
fish plates and scales, which are very rare. A few small lingulas
found in this horizon at the mouth of Pike creek on Lake Erie
are the only other fossils collected from these beds in the western
part of the State and they belong to the species found in similar
black shales higher in the Portage group, L. ligea Hall and
L. spatulata Vanuxem.
Plate 2
x
Cashaqua beds in the river gorge near Mount Morris. Upper part of cliff in
distance. Rhinestreet black shale
PORTAGE AND NUNDA QUADRANGLES 53
In the early reports of the Geological Survey this black shale
band was considered as the upper part of the Genesee black slate.
In United State. Geological Survey bulletin 16, 1885, J. M. Clarke,
for the reasons above stated, separated it from the Genesee slate
and considered it as a member of the Portage group under the
name “ Lower black band.” In New York State Museum bulletin
63, 1904, it was designated the Middlesex shale, from its abundant
exposures in the town of Middlesex, Yates co., from which locality
it is continuous westward maintaining its general characteristics,
but diminishing in thickness to 6 feet on the shore of Lake Erie,
where it is well exposed in the bed of Pike creek near its mouth
in the town of North Evans, Erie co.
The exposure of the Middlesex black shale in the cliff at the
mouth of the gorge is continuous in both banks for about 2 miles,
the dip bringing it down to the river level on the south side of the
“ Hogsback.” Other outcrops may be seen in the lower part of the
ravine 2 miles northwest of Mount Morris, at the mouth of Buck
run ravine, and on Cashaqua creek at the foot of the cliff at Sonyea.
Cashaqua shale
The beds included in this division were first described in the
Third Annual Report on the Fourth District, 1838, as they appear
succeeding the Genesee black slate in Yates and Seneca counties.
“The name Cashaqua shales first appears on page 390 of the
Fourth Annual Report on the Fourth District for 1839, where it is
‘said: “The group mentioned in the report of last year as suc-
ceeding the upper black slate, becomes on the Genesee a mass of
green crumbling shale of 110 feet thickness. It is exposed on
Cashaqua creek, hence the name Cashaqua shale.”!
In the final report of 1843, pages 226 and 227, after more fully
describing this division as it appears in the Genesee section, it is
added: “At the eastern extremity of the district and on the shores
of Seneca lake at Penn-Yan and other places, this rock consists of
a green shale with thin flagstones and interlaminated sandy shale.
It contains the same fossils ; and holding the same position as on the
Genesee it can be regarded only as the same rock. . . . Farther
east it is not recognized as shale at all, the mass consisting of thinly
laminated sandstones.” Tracing it west of the Genesee, it con-
*This Indian name derived from Gah-she-gwah, a spear, is also spelled
Coshaqua, Kishaqua, Kushaqua, Keshequa and Keshaqua. It is retained
here in the form used by Hall which is the spelling adopted in the geological
literature of New York for 7o years. The word is pronounced Kish-c-quay.
54 NEW YORK STATE MUSEUM
stantly presents the same features as on the Cashaqua but thins
down to 33 feet on the shores of Lake Erie.
The passage from the Middlesex to the Cashaqua shale is through
several alternations of light and dark layers in a few feet above
which horizon the black layers are infrequent and thin. They
reappear toward the top and after a few alternations like those at
the base become the homogeneous mass of black shale constituting
the Rhinestreet black shale, the succeeding member of the Portage
group. Fossils are not abundant in any part of the Cashaqua
shale, but a few may be found in all of the lighter beds and in the
upper and more calcareous olive shales they are fairly common.
Some large cephalopods are finely preserved in flat concretions
20 to 40 feet below the top of the formation.
Concretions usually a foot or more in diameter in a row at the
top of these shales in this section and further east have a layer of
calcareous matter 1%4 to 2 inches thick at the base composed of
fossils, sometimes in fine condition.
This is approximately the horizon of the Parrish limestone, a
thin calcareous layer of concretionary structure, continuous from
Canandaigua lake valley to Seneca lake and a reliable datum point
in the stratigraphy of that region.
The fauna of the Cashaqua shale is diverse and interesting. This
horizon is the normal seat of the peculiar fauna of the Portage
‘group, which is continued eastward without much variation but at
the west shows differences of composition [see Clarke, Naples
Fauna of Western New York]. .
In the general section the more common forms are:
Manticoceras pattersoni (Hall) Pterochaenia fragilis (Hall)
Probeloceras lutheri Clarke P. cashaqua Clarke
Tornoceras uniangulare (Conrad) Honeoyea major Clarke
Bactrites aciculum (Hall) Ontaria suborbicularis (Hall)
Orthoceras pacator Hall O. accincta Clarke
O. ontario Clarke Buchiola retrostriata (v. Buch)
O. filiosum Clarke Paracardium doris Hall
Phragmostoma natator Hall Palaeoneilo petila Clarke
Lunulicardium (Pinnopsis) acuti- Lingula ligea Hall
rostrum Hall Aulopora annectens Clarke
L. (Pinnopsis) ornatum Hall Melocrinus clarkei Williams
The Cashaqua shale is exposed in the walls of the gorge from.
near the mouth where the base is seen over the black beds for 6
miles to the north end of Smoky Hollow where the southwestern
dip brings it down to the river level. Opposite the lookout stations
along the “ High Banks” where the cliffs are 300 to 350 feet high,
> ets eee
solTeys goorqsoulyyy yortq Aq peddvo ‘soreys enbeyseo JO posoduiod si vspla oy, ‘SsyuURq YS
ey} WOAJ YSvO SULYOOT ‘UIVp STIAO|[, QUNOW SAO soTIM %%Z IEATI osoUeH) UI pueq 4v ., YOVq-SOF{,, EY} JO MOTA
PORTAGE AND NUNDA QUADRANGLES 55
the formation is displayed in a most striking manner, as a heavy
band of light blue gray in the middle of the wall contrasting strongly
with the black bands above and below it.
The mass of the unique “ Hogback” is composed of this shale
capped by the black Rhinestreet shale.
The ravine at Gibsonville affords an excellent opportunity for
examination of the upper beds and good exposures of the entire
formation may be found in the ravine 1 mile west of the mouth
of the gorge; in Buck run ravine, 1 mile southeast of Mount
Morris; along Cashaqua creek for 2 miles south of Sonyea, and on
the east side of the Canaseraga valley in the large ravines nearly
opposite Sonyea. The smaller ravines on both sides of the valley
present many good exposures of the upper beds and the contact with
the Rhinestreet shale appears at the roadside on the hill 114 miles
southeast of Groveland station, near the east line of the Nunda
quadrangle.
Rhinestreet black shale
[The Cashaqua beds from Schuyler county on the east to Lake
Erie are succeeded by a band of black shale with a few thin lighter
and mostly arenaceous layers intercalated at some localities
altogether differing materially in both structure and fauna from the
Gardeau group in which it was formerly included as described in
the reports of the Geological Survey of the fourth district. Its
strong contrast with the light blue Cashaqua beds below it, and the
flags and sandy ferruginous shales above it, makes it a distinct and
noticeable feature in the stratigraphy of western New York. It
was referred to by Clarke in United States Geological Survey
bulletin 16, as the “ Second Black Band” in the Portage group. In
New York State Museum bulletin 63, it is described as a Portage
unit, and on account of its constant exposure in the vineyard
region north of Naples known as “ Rhinestreet ” the name here used
was applied to it. i
It is 21 feet thick at Naples, but increases toward the west at an
average rate of about 2 feet per mile and on Lake Erie has a thick-
ness of 185 feet. In the Genesee river section the assigned thickness
is 53 feet. |
Fossils, except lignites, fish remains, conodont teeth and occasion-
ally a Spathiocaris and a few small lingulas are almost entirely
absent from these beds. The lighter interlaminated shales at the
top and bottom occasionally contain specimens from the Cashaqua
fauna.
56 NEW YORK STATE MUSEUM
The Rhinestreet black shale is finely displayed in the walls of the
gorge from the top of the north end of High Banks continuously
for 8 miles southward to the north end of the St Helena or Gardeau
Flats. ! ee
It is the cap rock of the “ Hogback” and is finely exposed at
Gibsonville, also on Buck run at and above the cascade and in
adjacent ravines; on Cashaqua creek for a mile midway between
Sonyea and Tuscarora; and in the ravine 2 miles northwest of
Mount Morris. .
On the east side of the valley it appears in several ravines 1 to
3 miles north of Groveland 'station and in the rock cut of the Dela-
ware, Lackawanna and Western Railroad, 114 miles southeast from
Groveland station. Very fine fish remains have been collected from
this locality. |
The list of fossils contained in the Rhinestreet black shale com-
prises the following species:
Palaeoniscus devonicus Clarke _ Prioniodus spicatus Hinde
Pristacanthus vetustus Clarke P. erraticus Hinde
Acanthodus pristis Clarke Spathiocaris emersoni Clarke
Polygnathus dubius Hinde Lingula ligea Hall
Hatch flags and shale
In the rather meager description of the “ Gardeau ee and
shales” in the reports on the geology of the fourth district some
reference is made to the difference between the character of the
lower and upper beds of the division.
This difference is more manifest in the Naples section specially
in regard to the faunas and the horizon of the change is marked by
a series of heavy sandstones that have produced an escarpment on
Hatch hill 275 feet above the Rhinestreet shale as exposed at the
foot of the hill.
In State Museum bulletin 63, the intervening shales and flags
between these sandstones and the Rhinestreet shale were fully
described and designated the “ Hatch flags and shale.”
In the Genesee section the formation is included between the
Rhinestreet black shale and the bank of thin sandstones that is seen
in the cliff on the east side of the Gardeau Flats, coming down to
60 feet above the river at the east end of the St Helena bridge and
to the river level at the mouth of Wolf creek, embracing 209 feet
of shales and flags. The shales are in thin layers many of them
being black and slaty, others blue and fissile or olive, coarse and
sandy. The general aspect of the rock walls in this part of the
——— ae ~~
—— ——
| | TMOYS ATJOUTISIP SI SOeys YoryTq
qoorJSoulyYy SULATIOAO oY puv soreys enbeyseD oy} Jo JowJUO0D EY, ,,, YoRq-SOP,,, oy} JO epis ysveyynog
Plate 5 :
Rock cut in Cashaqua shales. Cashaqua creek
PORTAGE AND NUNDA QUADRANGLES 157
ie
gorge is made dark and rusty by the ferruginous characters of the
ser shales and sandstones. .
_ The flags in these beds are smooth.and even on the lower surface
except for the presence of casts of depressions in the soft mud
beneath, on which they were deposited in the shape of short
peer ridges lying at all.,angles. These bodies have been known
‘as Fucoides graphica. The upper surface of the flags is
us sally shaly. Fossils except plant remains are very rare, though
some of the lighter colored shales in the lower part contain:
Manticoceras pattersoni (Hall) Ontaria suborbicularis (Hall)
Probeloceras lutheri Clarke Palaeotrochus praecursor Clarke
Orthoceras pacator Hall Buchiola speciosa (v. Buch) and a
Phragmostoma natator Hall few other forms.
_ Besides the exposure of these Hatch beds for 8 miles in the cliff
along the river from opposite Gibsonville to the mouth of Wolf
creek, they may be seen along the Silver lake outlet 2 miles below
Perry; in the upper part of the ravine 2 miles northwest of Mount
Morris; along Buck run above the falls to the first highway bridge;
on Cashaqua creek and at Tuscarora a mile below; also in the
ravines at West Sparta and in nearly all of the ravines on the east
side of the Canaseraga valley within the limits of the Nunda quad-
rangle. 3
q Grimes sandstone
_ At the mouth of Wolf creek a band of thin sandstones separated
by hard dark shales, altogether about 25 feet thick, overlying the
Hatch flags and shales comes down to the bottom of the cliff. It
‘is 60 to 85 feet from the base of the cliffs at the east end of the
$t Helena bridge and is prominent in the eastern rock wall opposite
the Gardeau Flats, 1 to 2 miles below St Helena.
It is here essentially barren except for plant remains, and it is
“not a very well defined nor significant feature of the Portage section
m the Genesee river or further west, but toward the east in the
ed and Naples valleys the sandstones are much heavier
an nd contain brachiopods and other forms not found in the Portage
ids of the western part of the State, though most of them are
‘common in the “Ithaca” beds of this horizon and that of the
Hatch flags and shales in Tompkins county and farther east.
At Naples the characteristic lamellibranchs and many of the other
te orms composing the Naples fauna that occur more or less abund-
mtly up to the base of this band have not been found above it.
This formation was first described as a member in the Portage
58 NEW YORK STATE MUSEUM
group in State Museum bulletin 63, and designated Grimes sand-
stone from its exposure in Grimes gully at Naples, N. Y.
Other outcrops of these sandstones may be seen in several small
ravines west of Smoky Hollow and on the Silver lake outlet 1%
miles below Perry, also in the gullies north of Groveland station
and south of West Sparta.
Gardeau flags and shale .
As considered in this bulletin, this formation consists of an ex-
tensive series of flags or thin sandstones and shales occupying that
part of the river section between the Grimes sandstone at the
mouth of Wolf creek and the base of the heavy sandstones at the
top of the Upper falls, with an aggregate thickness of 344 feet.
These rocks constitute the most striking part of this famous
canyon. On the south side of the mouth of the Wolf creek ravine
the vertical cliffs rise 250 to 300 feet in which the bands of black,
blue gray and olive shales, and the greenish or blue sandstones of
varying thicknesses and in irregular succession are displayed in the
most effective manner.
The lower beds, principally shales, are accessible in times of low
water in the lower part of the Wolf creek ravine, and some of the
lighter colored layers are fossiliferous.
Midway in the cliffs for 2 miles south of Wolf creek the even
stratum of sandstone that is the platform of Table rock at the top
of the Lower falls, 70 feet high, is seen. Below this stratum down —
to the bottom of the falls, there are five layers of black shale agere-
gating 9 feet in thickness, intercalated at irregular intervals in 57 |
feet of gray shale and a few thin flags. Above it the sandstones —
are more frequent and increase in thickness, and in the walls below |
the Middle fall compose a considerable portion in the sedimentation.
They are mostly not more than a foot or two in thickness, cee
and layers of both light and dark shales recur up to the top of the |
formation.
In the broad slope of rock on the west side of the river extending
from the top of the Middle to the bottom of the Upper falls 19
feet of shales and flags are accessible and 20 feet more on the west
side of the waterfall can easily be reached.
For 51 feet above the bottom of the Upper fall the rock is prin-
cipally soft with seven thin layers of dark or black shale inter-
stratified between light shales or thin flags. One stratum of rather |
-a
shaly sandstone 2 feet, 5 inches thick is 19 feet above the base of
the section and is separated from a similar but slightly more com-
SOTVYS puR Sov Nvepivey ‘SLIT WeTH ‘ST[eJ IaMoT MOTEq 8S.105
Cathedral rock, below the Flume, Glen Iris. Gardeau flags and shales
PORTAGE AND NUNDA QUADRANGLES 59
"pact layer 3 feet, 6 inches thick by 5 feet, 4 inches of soft shale
_ mostly dark.
This sandstone is succeeded at the top \ the formation by 19
feet, 8 inches of light and dark shales with a few thin flags, overlain
by the stratum of light blue gray sandstone 7 feet thick that is the
basal layer of the next higher member of the Portage group, the
"Nunda sandstones. The Gardeau flags and shales are the lowest
“rocks exposed on the Portage quadrangle in the Oatka creek or
‘Warsaw valley. In the large ravine of Stony creek or Fall brook,
-¥% miles southwest of Warsaw 235 feet of these beds are finely
_ exposed below the Erie Railroad. They are, as a whole, noticeably
softer than in the Genesee river section and there are fewer sand-
_ stones except at the top of the falls, where a hard stratum 1 foot
; thick has been denuded of shale for the space of a few square rods,
‘and is locally known as Table rock. It is not, however, in the
same horizon as the Table rock at the Lower Portage falls.
In Gibson’s glen, near South Warsaw, 150 feet of the upper beds
are exposed, and a somewhat less thickness of the same up to the
top of the formation in the ravine of Oatka creek between Newburg
and Rock Glen. :
_ In the Nunda or Cashaqua creek valley the small ravines on the
side of East hill opposite Nunda and on the west side below Brooks
_ grove, show partial sections of these beds, and Wildcat gully cuts
‘through the entire formation.
_ The upper parts of the rock gullies on the west side of the
( anaseraga valley above West Sparta and nearly up to Byersville
are in the Gardeau beds, and they are exposed under similar con-
ditions on the east side above Groveland station.
_ The fauna of the Gardeau beds on these quadrangles is not an
‘extensive one, but it is made specially interesting by the fact that it
‘is composed of several species that first appeared in the Genundewa
limestone and were more or less common in the Cashaqua, with
‘additions from the Portage fauna on Lake Erie, and, east of the
‘Tiver, some members of the Ithaca fauna that do not appear in the
exposures in the gorge, nor in this horizon further west.
Fossils except plant remains are usually almost entirely absent
_ from these sandstones on the Portage quadrangle but Table rock in
the Fall brook ravine, Warsaw which is in two parts, separated by
‘a thin seam of shale, bears on the surface of the lower part scores
‘of the little lamellibranch Buchiola retrostriata and
“Several other species abundantly. Some flattened concretions in a
60 NEW YORK STATE MUSEUM
bed of soft shale at the mouth of Gibson’s glen contain some
beautifully preserved fossils, mostly small specimens of Manti-
coceras rhynchostoma Clarke and similar concretions
occur elsewhere in this horizon but by far the larger part of the
fossils collected from the Gardeau beds have been found in layers
of light blue or olive soft shale, generally but a few inches thick. —
But few of them are conveniently accessible to collectors, but the
lower one may be reached at the mouth of Wolf creek and others
a mile farther up the ravine.
At the top of the Lower Portage fall, a 10 inch layer immediately
beneath Table rock is quite fossiliferous and a thinner layer Io feet
lower contains a few lamellibranchs and Manticoceras ©
rhynchostoma occurs though very rarely, just above the ©
I2 inch sandstone at the top of the Flume. _
In 1906 a fall of rock from 60 feet up in the cliff on the east —
side 40 rods above the Lower fall, brought down a part of an —
extensive bed of plant remains in which were many fragments of .
lepidodendron. A thin layer at water level half way between the |
Middle and Upper falls has afforded a number of fine specimens ~
of Manticoceras oxy Clarke and other species, while similar |
layers occur a few feet higher.
Although no brachiopods have been found in these beds in the —
gorge it is quite possible that some of the considerable number —
common in this horizon in the Naples valley may have extended as —
far west as this and their remains be buried in the inaccessible strata —
of the cliffs. A thin calcareous seam exposed by the roadside on
Quarry hill 1 mile south of Nunda and stratigraphically near the
top of the Gardeau beds, is composed of crinoid stems and frag-
ments of brachiopods, and a calcareous sandstone 3 inches thick
exposed by the side of the river road 2 miles north of River Road
Forks and in the lower part of this formation contains Ambocoelia
in large numbers, also Chonetes and fragments of Leptosiaa less
abundantly, all exceedingly small.
The following is a list of the more common fossils in the Gardeau
beds on these quadrangles:
Entomis serratostriata Sandberger Bactrites aciculum (Hall)
E. variostriata Clarke Styliolina fissurella (Hall)
Manticoceras pattersoni (Hall) Phragmostoma, natator Hall
M. oxy Clarke Loxonema multiplicatum Clarke
M. rhynchostoma Clarke Palaeotrochus praecursor Clarke
Tornoceras uniangulare (Conrad) Lunulicardium bickense Holzapfel
Orthoceras pacator Hall Honeoyea erinacea Clarke
Plate 8
} ‘
Wea
ris.
Lower falls and ‘‘ Flume,” Glen I
Part of the Lower falls at Portage from Table rock. Gardeau flags and shales
Ea ee ee ae ee ee
PORTAGE AND NUNDA QUADRANGLES 61
H. major Clarke B. lupina Clarke
H. desmata Clarke Paracardium doris Hall
Posidonia attica (Williams) Pterochaenia fragilis (Hall)
Ontaria suborbicularis (Hall) Cladochonus
O. clarkei (Beushausen) | Lignites
Euthydesma subtextile Hall Fucoides graphica Hall
Buchiola retrostriata (v. Buch) F. verticalis Hall
Nunda sandstone
A stratum of sandstone 7 feet thick, the bottom of which is 28
feet below the top of the Upper fall is the basal layer of this sub-
division. It is succeeded by 7 feet of shales and thin flags, overlain
by the somewhat shaly sandstone 13 feet, 6 inches thick seen at the
crest of that fall.
A bed of hard blue shale 4 feet, 4 inches thick overlies this sand-
stone, another 12 feet higher is 2 feet thick and a third 70 feet
above the top of the falls is 6 feet thick with an 8 inch layer of
sandstone in the upper part.
Except these three beds of shales and a few thin shaly partings
between the heavy layers the formation as exposed in the Genesee
river gorge section is composed entirely of light blue gray sand-
stone in layers from 3 to Io feet thick, some of which are calcar-
eous to a greater or less degree, and hard, while others are schistose
or coarsely shaly in many laminations. Large and usually obscurely
defined concretions or burls occur in some of the layers.
The cliffs at Portageville by long exposure have weathered to a
yellowish or olive-gray color, and that is commonly the color of
these beds in old outcrops everywhere, but when newly quarried
the rock has a handsome blue gray tint and is popularly known as
_ “Dluestone.” The more compact layers are extensively quarried on
_ the west side of the river 114 miles south of Portageville by the
Portageville Bluestone Co., and at Bluestone by the Genesee Valley
Bluestone Co., and near Rock Glen by the American Bluestone Co.,
and the Warsaw Bluestone Co., sawed into flagging and house
trimmings, the handsome color of the rock combined with its
durable character making it extremely popular for such use and of
_ considerable importance economically.
The 6 foot bed of shale seen at the line of the Pennsylvania
Railroad at the south end of the high Erie Railroad bridge, con-
tains large numbers of small irregularly shaped calcareous con-
* o94en"
cretions that give the bed a distinctly nodular expression not seen in
shales east of these quadrangles but common in the western part
62 NEW YORK STATE MUSEUM
of the State. This band appears in the quarries at Portageville
and also at Rock Glen, and may serve as a datum by which to
determine the place, in the series, of the more valuable quarry stone
layers. It may be seen on Quarry hill at Nunda at the reservoir.
A thinner layer of the same character appears high up in the
quarry wall here, but it thins out toward the west and is scarcely
noticeable in the river gorge. The nodules are common also in
the 2 feet of shale near the bottom of the formation at Portage-
ville. :
Next to that of the gorge section and the quarries mentioned
the best exposure of the. Nunda sandstone on these quadrangles
is on Quarry hill 1 mile south of Nunda and along the road to
Dalton. It crops out occasionally on the hill east of Nunda along
the wall to Byersville and in small ravines and is well displayed in
Wildcat gully in the northeast corner of the town.
It is exposed along Wolf creek below Castile and for a mile
west of the Erie Railroad ae Relyea creek and Stony creek near
Warsaw.
Lignitic plant remains are common in the sandstones, sometimes
in sufficient quantity as to form thin coaly seams of small extent.
The lignites are usually fragmentary and rarely well enough pre-
served to allow identification of species. |
Manticoceras oxy Clarke, M. rhyme
Clarke, Aulopora, Orbiculoidea sp. Crinoid stems, Fucoides
verticalis and a few small representatives of the Gardeau
fauna, constitute the fauna of this formation in the river section,
but in the eastern part of the Nunda quadrangle thin seams of the
comminuted shells of brachiopods occur and in the Naples valley
these rocks contain a well developed Chemung fauna.
The Nunda sandstones are prominent in the stratigraphy of
western New York from Chemung county to Lake Erie. The
formation, while retaining its character as a mass of homogeneous
barren sandstones, thins out rapidly west of Wyoming county and
on the shores of Lake Erie south of Portland harbor where it dips
under the water it is but a few feet thick.
Toward the east it becomes gradually less homogeneous and more
assimilated to the adjacent formations, but may be traced in numer-
ous outcrops as far east as Chemung county. In the vicinity of
Naples these sandstones contain calcareous masses of fossils, mostly
belonging to the fauna of the Chemung rocks. One of these out-
cropping in High point, a rock bluff 3 miles west of the village,
SoTVYS pUR SOR NvepIeH “OovI10g ‘ST[VJ IaMOT Jo pus toddq
AT aA1PT +r
SOTeYS pure sovy ne
‘YSty 199F OOS WeYF oO OP9IIT V SI [[VM Yoor oy
TT a1yPT_
apres
‘ST[VJ TOMOTT pur
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PORTAGE AND NUNDA QUADRANGLES 63
' contains 22 species of brachiopods among them Spirifer
-disjunctus Sowerby, besides many other forms, and another
lentil 3 miles south is -a mass of fossil sponges and Chemung
brachiopods, forms that did not appear in the Genesee valley sec-
tion till after more than 200 feet of sediment had been deposited
above this horizon. The sandstones at the top of the formation
_ here pass gradually into soft sandy shales. The exact point of
contact with the succeeding formation is covered at Portageville but
is slightly exposed by the side of the Quarry hill road 114 miles
south of Nunda. The strata included in the Nunda sandstones as
considered in this bulletin have an aggregate thickness of 215 feet.
In various recent publications the singularly interesting fact has
been brought to notice that an essential difference in classification
of the upper rocks of this Devonic series results from the inde-
pendent consideration of the stratigraphic and the paleontologic
q evidence. In paleontology the Portage group here extends upward
_ to include a mass of olive shales with some sand having a thickness
of several hundred feet, and the upward extent of this fauna in the
_ Genesee section is characteristic of its range throughout the region
farther west in the State. But at the east, in the Canandaigua-
Naples meridian, this fauna disappears practically or entirely at a
horizon below that of the Nunda sandstones. ‘These sandstones
have been traced almost foot by foot between these meridians, and
the stratigraphic continuity of the Nunda sandstones of the Genesee
section with the High Point sandstone of the Naples section is
beyond question. The seeming inappropriateness of a twofold
designation for the same geologic horizon is dispelled by the entire
difference in the contained faunas at these distant sections. In
_ paleontology the High Point sandstones carrying a brachiopod fauna
with Spirifer disjunctus are of Chemung age, the Nunda
_ sandstones of Portage age. We therefore have in the Nunda sand-
_ stones of the Genesee valley a member of the Portage group which
lies at the base of the Chemung group farther east. Another and
still higher member of the Portage group is also present in this
_ section and its presence and probable value were indicated by Hall
in 1839 [Annual Report, p. 392].
The two groups just described (Gardeau and Portage) occupy
a thickness of more than a thousand feet and are interposed
“between the Cashaqua shale and the Chemung group. Indeed,
if we consider the Chemung group as commencing with the occur-
64 NEW YORK STATE MUSEUM
rence of its characteristic marine fossils, then several hundred feet
more of rocks may be noticed as intervening between the upper
Portage rock and that group. The rock succeeding the upper
Portage rock consists of ‘greenish olive, sandy shale, or very shaly
sandstone, never slaty. The only fossils seen in this rock is a
species of fucoides with a striated surface, and these are by no
means numerous. This is succeeded by a dark, nearly black sandy,
highly micaceous shale with septaria. It contains iron pyrites and
where exposed is of an iron rust color externally. Some thin
masses of gray sandstone are interstratified which contain fossils
referable to the Chemung group.
[p. 402] Succeeding the black micaceous shale are the sandstones
and shales constituting the Chemung group which is everywhere
visible in the ravines and banks of streams. Its northern limit
extends through the southern part of the towns of Centerville,
Hume, Grove and Burns. In this county more particularly along
the Genesee river and west, the group differs in lithological char-
acters and consequently in some degree from the same rocks in
Steuben and Chemung.
From these quotations it is clear that though Hall conventionally
classified all of the rocks succeeding the Portage (Nunda) sand-
stones for a thickness at least as great as appears on these quad-
rangles, as belonging to the Chemung group, he directed attention
to the fact that they might be subdivided as follows:
1 Olive shales and shaly sandstones at the base.
2 Micaceous shales with thin sandstones containing brachiopods.
3 Heavy sandstones and shales which, lithologically are very
similar in character to the strata referred to as constituting the
Chemung group at the type locality.
Sufficient data have not yet been obtained on which to decide
whether divisions 2 and 3 should be considered as separate geologi-
cal units, but it is not improbable that further invesigations may
demonstrate that they are such.
The beds of division 1 are known as the
Wiscoy shales and sands
These shaly olive beds were described as a unit in the New York :
geological series, and the relations of the fossils found in them
discussed by Clarke in the 16th Annual Report of the State Geolo-
gist of New York, 1898, and the name “ Wiscoy shales and sands ” |
applied to them on account of their favorable exposure at the falls
of Wiscoy creek at Wiscoy, N. Y.
The stratigraphy of these beds was shown in detail in diagrams
accompanied by description, by Luther in New York State Museum
bulletin 69, 1903.
SoTBVYS puB Soey nveprey oyy jo 41ed zoddn oy} Uy], “'s[[eV} Jamory] pue s[pprIp{ 9Y} Woemyoq eS10y
7T AIYPT ST
Plate 13
The Middle falls at Glen Iris. Gardeau flags and shales
PORTAGE AND NUNDA QUADRANGLES 65
South of the sandstone cliffs at Portageville the course of the
‘Genesee river winds through a broad valley in which the only
exposures of these soft beds are to be found in the various excava-
‘tions in the adjacent hillsides.
The basal layers may be seen in the ravine 1%4 mile south of
Bluestone; and at the falls of Wiscoy creek at Wiscoy the floor
and walls of the ravine display 135 feet of the middle and upper
beds. Near the top of the north walls above the falls the calcareous
‘sandstones occur that succeed this formation and are the lowest of
‘the “coarse sandstones with fossils of the Chemung group,” re-
mrerred to by Hall, in the Genesee river section. This band of
sandstones comes down to the river level 5 miles south of Wiscoy
-and 1 mile south of Fillmore at Long Beards Riffs where it makes a
low cascade and is exposed on both sides of the river. It was
described and the designation “Long Beards Riffs sandstone ”
applied to it by Luther in New York State Museum bulletin 60,
1903. The lower beds of the Wiscoy division are mostly coarse
blocky shales or soft sandstones with an occasional flagstone. In
‘the middle and upper parts the sedimentation is generally finer, and
‘there are several layers of black slaty shale one of which is 6 feet
‘thick. An 8 foot bed of nodular shales lies next below this black
bed and concretions from an inch to 3 feet in diameter occur
throughout the entire formation. |
_ Nearly all of the beds are calcareous to a greater or less degree
and on the whole greatly: resemble the Cashaqua shale. This re-
‘semblance becomes even stronger toward the west, but is lost
3 a certain extent toward the east owing to the increase of
-arenaceous matter.
_ The exposure at Wiscoy and in the ravines on the east side of
the valley 1 to 3 miles farther south afford the best opportunities
for examination of the Wiscoy beds. They are also exposed along
Stony creek 2 miles west of Warsaw and slightly along the upper
teaches of Relyea creek and Oatka creek, also east of the Genesee
Valley for % mile north of Hunts along the Nunda road, and by
the roadside 1 mile southwest of Dalton. Small outcrops are com-
‘mon by the roadsides and in the ravines on the slopes of the hilly
Tegion east of Nunda.
_ In Steuben county where these beds are coarser they contain
many Chemung brachiopods and it is probable that the same species
Occur in this horizon in the eastern part of the Nunda quadrangle,
66 NEW YORK STATE MUSEUM
though owing to a lack of favorable exposure they have not been
observed.
The fauna of the Wiscoy is a sparse one in both species and
individuals.
The following have been collected from Wiscoy creek ravine
and the gullies on the east side of the valley 2 to 4 miles farther ~
south:
Manticoceras oxy Clarke Lunulicardium (Pinnopsis) wiscoy-
M. rhynchostoma Clarke ense Clarke
Orthoceras sp. Paracardium doris Hall
Pleurotomaria sp. Zaphrentis sp.
Hyolithus neapolis Clarke Lingula ligea Hall
Buchiola retrostriata (v. Buch)
Chemung group
In discussing this division in Museum bulletin 81, 1905, (Watkins
and Elmira Quadrangles) the following commentary was made on
the general value of the term:
The term Chemung has been applied with such a breadth of mean- —
ing in New York stratigraphy that faunally and stratigraphically it —
no longer meets the requirements of precise expression. The forma-
tion has been, in a general and vague way, regarded as that mass —
of arenaceous deposits lying above the Portage of western New |
York and the Ithaca of central New York, from which there is,
as is now known, a transition lithologically so gradual as to make |
a separation a pure convention. In respect to fauna the “ Chemung
group” has been commonly regarded as well defined by the pres-
ence of a notable series of species specially brachiopods, lamelli-
branchs and dictyosponges, all of which have been in a way re-
garded as centered about the species Spirifer disjunctus
and the horizon, as a whole, including a thickness of from 1000
to 1500 feet of strata, regarded as the horizon of Spirifer dis
jinetyu si! “Fhis conception, as we have heretofore explained, ia
misleading, vague and inaccurate. The horizon of Spirifer
disjunctus follows close on the change from the Naples fauna
in western New York at a high altitude above the base of the
Portage formation. In central New York there is no such change
but the gradation from the Ithaca fauna out of the Hamilton fauna
upward into the association which carries species elsewhere con-
current with Sp. disjunctus is very easy and it is extremely
difficult to draw a division plane anywhere except on the basis of
refined distinctions into successive faunules. Spirifer dis-
junctus in this eastern region did not appear till this period
of “Chemung” deposition was well nigh over. For a precise use
of this term Chemung therefore we are thrown back on the
: Plate 14
i
|
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|
4 * * i
ee"
“T
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4
\
Middle falls at Glen Iris, from the west side. Gardeau flags and shales
SOTeys puv’ Sob NVIPITeL) “FUolL of WO YICA YILOMYOJoT
‘punoisyoeq oy ut stTey toddq oY} eaoge ospliq pvorIey olig Oy, “MOTE 96105 9Y4 pu ST|eF S[PPI[L PUI,
co oreseh SSS Eines |B
pean ss ik = a
|
eee
‘ PORTAGE AND NUNDA QUADRANGLES 67
original employment of the name and we here cite the explanation
of the term as first used by Professor Hall, taken from the Third
Report on the Fourth Geological District, 1830, pages 322-24:
me. Lhe tops of the hills and high erounds in the towns of Erin,
'Veteran and Catlin, display a group of rocks and fossils very
distinct from those last described. The essential difference is the
lithological characters of the sandstone of this group in the absence
of argillaceous matter in most of the layers, these being nearly a
“pure silicious rock, harsh to the touch, and generally of a porous
texture; while still a large proportion of the mass consists of com-
pact shales and argillaceous sandstones of a softer texture than
“those below. The surface of the sandstone layers is rough, while
those below are smooth and glossy, and being: never rippled, prove
Bthat the rocks were deposited in a quiet sea.’
In the previous chapter we have referred to an already recognized
“necessity of removing from the Chemung division of the Genesee
valley a lower portion which Professor Hall himself anticipated
Beicht have to be excepted therefrom on stratigraphic grounds only.
With the Wiscoy beds eliminated there remains thereabove in this
"section 400 feet of sandstones and shales, not differing greatly from
‘the Portage beds in appearance nor lithologically, though the sand-
‘stones are usually light olive-gray in color and more micaceous.
Thin layers of impure limestone resulting from aggregations of
brachiopods and other fossils occur occasionally in the sandy layers
“but are most common in the upper beds. The shales are in all
"variations and shades of color from light blue gray and olive to
deep black. Rows of small calcareous concretions occur in some
of the lighter shales, and larger, but less clearly defined masses of
_concretionary ehaeatier are in a few of the heavier sandstones.
_ The stratum containing brachiopods at Long Beards Riffs and
“Wiscoy falls is in the lower part of a band of sandstones and shales
exposed at Mill’s Mills and along East Koy creek, a mile north of
Lamont. Soft shales prevail in the succeeding 400 feet of strata
‘though there are several lentils of sandstone embraced in this part
‘of the section. Exposures of this horizon in the vicinity of Pike,
“show mostly light shales that become rusty on exposure between
thin rough flags 1 to 3 feet apart. In the Dingman quarry I mile
“north of Pike a 12 foot band of sandstones is exposed that is about
200 feet higher in the strata than the Long Beards Riffs lentil.
These sandstones are also exposed along the Allegany road a mile
‘southwest of Pike, where one of the layers contains a calcareous
‘mass of fossils and after long exposure weathers dark brown.
q
——" eee
:
68 NEW YORK STATE MUSEUM
There are many small exposures of this part of the Chemung group
along the roadsides and in small gullies on these quadrangles, but
none that show more than a fraction of the rock section. It is
well displayed, however, along Caneadea creek and in other ravines
on the next quadrangle south of the Portage.
At 1700’ A. T. on the Allegany road 4 miles southwest of Pike
there is manifest a considerable change in the conditions of sedi-
mentation, soft shales no longer predominating, but a series of
flags and sandstones, many of which contain brachiopods in large
numbers, appears and is exposed along the roadside showing a
thickness of 150 feet or more, above which the rocks are covered
by drift, but blocks of compact quartzitic gray sandstone, very
coarse in structure and in some parts having the composition of a
fine conglomerate, are scattered over the fields or built into the
fences in such quantities as to make it evident that it is the bed
rock in the vicinity of the crossing of the Allegany road and the
east and west road near the south line of the quadrangle. There
is no other favorable exposure of these sandstones on these quad-
rangles but they are amply displayed in the Belfast quadrangle.
Fossils are not abundant in the strata succeeding the Wiscoy
shales for 400 feet except in a few thin seams in the lightest shales
and in the heavier of the sandstones. The following species have
been collected from the stratum succeeding the Vo shale as
Long Beards Riffs and Wiscoy:
Spirifer disjunctus Sowerby Atrypa aspera Hall
S. mesacostalis Hall Camarotoechia sp.
Liorhynchus multicosta Hall Orbiculoidea alleghania Hall
Productella lachrymosa Conrad Orbiculoidea cf. media Hall
P. speciosa Hall Ambocoelia umbonata (Conrad)
P. hirsuta Hall Lingula cf. melie 7
and several unidentified species. These are the prevailing forms
that appear in the lower Chemung beds on these quadrangles and
most of them continue up into the heavy sandstones where they are
much more abundant and where other species are added to the
fauna.
Dip
The rocks of these quadrangles show very little evidence of dis-
turbance except in an even gentle dipping toward the south-south-
west. The line of contact between the Moscow shales and Genesee
slate has a westward declination of about to feet in the 55 miles:
;
5
;
;
‘
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.
:
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soleys pue ssvpyp nveprey teddQ ‘eoplaq prorpley olaq oy} pue s[[eq 19ddQ 09 Jo Mola
QI 93e[d
PORTAGE AND NUNDA QUADRANGLES 69
between its exposure at Moscow and on the shore of Lake Erie.
This westward dip is increased by the thinning out of the Genesee
and Portage beds, producing a different rate for each contact line.
For the top of the Nunda sandstones the average is about 8 feet
P The average southern dip is 20 to 22 feet a mile and toward the
south-southwest 30 feet a mile. This appears to. be slightly in-
creased in some of the quarries, possibly due to the relief from
pressure following the excavation of the deep valleys on the sides
of which they are located. 7
PLEISTOCENE HISTORY OF THE GENESEE WV
IN THE PORTAGE DisTaice
LY
HERMAN L. FAIRCHILD
Evolution of western New York drainage
Any adequate discussion of the preglacial history of the Genesee
river in its broader relations would involve the whole problem of the
changes and adjustment in the drainage of the area of western and
central New York and northern Pennsylvania during all time since
the later Paleozoic. This is a large problem which has not been
seriously attacked and one which requires much study. For the
purpose of the present writing we shall be content with the briefest
presentation of the elements of the problem.
It would seem certain that the primitive and consequent drainage
of the western half of the State, along with the northern and western
part of Pennsylvania, must have been southward or southwestward
when the region was slowly uplifted from the seas as a coastal plain, —
bordering the old lands of Canada and the Adirondacks. Such
elevation probably occurred not later than the Subcarboniferous. |
Many of our broader valleys, specially those with a southward or
southwestward trend, are probably an inheritance from that earliest —
drainage across the uplifting plain. In the course of time the at-
titude, structure and composition of the rock strata, along with the
up and down movements of the land, influenced the disposition of
the drainage.
In the Ontario region a great thickness of weak rocks permitted
the secondary or subsequent streams having east and west courses, —
along the strike of the strata, to develop and strengthen at the ex-
pense of some of the older and trunk streams. Eventually some
of these subsequent streams united to make a great main or trunk
stream, flowing either east or west, and so there was developed by —
atmospheric and stream work the great Ontario depression. With
the deepening of the east and west Ontario valley the drainage along
the southern side was reversed by streams developing nore
flow toward the Ontarian river. In later geologic time probably
70
athe ge alt bi ag!
PLEISTOCENE HISTORY OF THE GENESEE VALLEY v/a
most or all of central New York was included in this reversed
(obsequent) drainage, having northward flow down the inface of the
Allegheny table-land. The valleys of the Finger lakes represent the
work of such northward drainage,! but the most conspicuous and
the longest example is the Genesee river. 7
During the long process of adjustment of the drainage there
were great changes not only in land altitude but also in the climatic
factors. Recently the Pleistocene ice sheets have plowed across the
region and in a capricious manner have left some valley stretches
filled with rock rubbish while other long stretches have been unfilled,
or even scoured and cleared. Not only has the preglacial topog-
raphy been thus obscured and the drainage diverted, but still greater
interference with the old drainage was produced by the damming
effect of the ice itself, in forcing the drainage into new lines, either
southward or in directions along the ice front.?
The Genesee, as above noted, is the longest stream in New York
which retains its preglacial northward course. It has persisted in
its northerly course in spite of obstructions and diversions, for a
little thought makes it evident that the damming and diverting effect
of the glacier must have been to destroy the original northward flow
rather than to produce such flow.
Diversions of the river. Buried channels
In the course of the Genesee river there are three stretches where
its valley shrinks to a narrow steepwalled ravine or canyon. One
is at Portage, a second near Mount Morris, and a third at Rochester.
The first two are parts of a single diversion of the river. Above
Portageville and below Mount Morris the valley is broad and flaring
and is evidently the result of weathering, storm wash and stream
transportation during millions of years. The canyons represent the
same kind of geologic processes as the open-valley stretches but
only a small fraction of the time. Quantitatively the canyons are
inharmonious with the rest of the valley, and have long been recog-
nized as the very recent or postglacial work of the river where it has
been forced from its old valley into a new path.
Logically it must follow that for each of the new stretches of the
river course there must be a corresponding deserted stretch of the
ancient valley. As to the cause of the changes in the river’s course
there is no disagreement among geologists, it being the interference
MtSee N. Y. State Mus. Bul. 45, p. 31-54; Geol. Soc. Am. Bul. 16: §5-56.
2For illustration of such glacial drainage see N. Y. State Mus. Bul. 106,
72 NEW YORK STATE MUSEUM
of the ice sheet, as described above. The deserted and mofe or less
drift-buried stretches of the older valley must connect the ex-~
isting open, mature stretches, passing around the new, ravine
stretches. ’
The criteria for locating the abandoned stretches are as idtiowsa
(1) Direction: which would be expected to lie in fairly direct line
connecting the open or unobstructed stretches. (2) Width: which
should correspond to that of the old, open valley, making allowance
for any difference in the character of the rocks. (3) Walls: which
should have slope and height similar to the open stretches. (4)
Depth: the original bottom of the deserted stretches must have been
in accord or graded with that of the open parts. In want of deep
borings sufficient to fully prove the location, depth and form of the —
buried stretches we have to rely at present on the general form and
relation of the broader valley features and the exposures of rock,
While these are not entirely satisfactory yet they are probably suffi-
cient to show the main facts of the preglacial drainage.
Rochester district. Somewhere between Avon and Rochestel
the Genesee river leaves its old valley and enters its modern course,
which becomes at Rochester a rock canyon with three cataracts, cut
in Niagara, Clinton and Medina strata. The ancient and wider
channel must have had a northward trend and somewhere must have
crossed the Niagara scarp in order to join the river or lake whick
occupied the Ontario depression. From the St Davids valley te
Sodus bay there is no break in the horizontal strata which could
possibly have carried a large stream for a long time except the gap
now occupied by Irondequoit bay (or lake). Here is an open valley
over a mile wide, in hard rocks, and extending southward as <
traceable depression some 15 miles. The depth of the Irondequoit
valley to rock is unknown but the depth of water is given as 87 feet
The rock bottom of the old valley must‘be graded to the depth of
the Ontario basin which runs into hundreds of feet a few miles ou
from the south shore. ‘
The conclusion is unavoidable that here we have a portion of d
old, preglacial Genesee valley, and the most northerly stretch nov
above the waters of Ontario. From the neighborhood of Fishers
in the Irondequoit valley, westward to the Genesee valley near Wes
Rush, or to the mouth of the Honeoye creek, the old valley is.
completely obscured that no confident suggestion of its course ¢
be based on surface features. It appears most probable that th
course of the river had been adjusted to the underlying rocks an
Swe ee
Nunda and part of Portage quadrangles
PLEISTOCENE HISTORY OF THE GENESEE VALLEY . 7s
that a few miles north of Avon the channel bent eastward along
the outcrop of the very soft Salina shale, similar to the present
streams on the latitude parallel between Buffalo and Syracuse,
This east and west stretch of the ancient valley, lying athwart the
direction of the ice movement, was the part most filled by the
glacial drift.
' Portage-Mount Morris district. The canyons at Portage and
Mount Morris together with the 8 miles of narrow intervening
valley represent a single diversion of the river. Evidently the ravine-
like valley from St Helena to Gibsonville is older than the canyons
at the two ends, being V-shaped and flaring, although the rocks
are as resistant as those of the Mount Morris canyon, locally
called the ““ High Banks.” Yet this valley is decidedly too narrow
to have been a part of the Genesee valley, and is entirely out of
harmony with the open valley above Portage and below Mount
Morris. We must conclude that the St Helena valley belonged to
some smaller or tributary stream.
The St Helena creek, as we may name the preglacial tributary,
probably flowed south and entered the Genesee river 2 miles east
Df the Portage viaduct, near the Lewis corners [see map]. Ina
similar relation the depression followed by the Erie Railroad north
to Silver Springs and including the valley of Silver lake probably
drained south and joined the Genesee valley north of Portage by
the break in the west wall at that point. This gap in the rock wall
is too small to represent the old valley of the river, as suggested
vy Grabau,! but undoubtedly is the junction of a tributary valley.
dis suggestion that the old valley led northwest and comprised the
Warsaw-Wyoming or Oatka creek valley can not be maintained.
First, the break in the rock wall at Portage is insufficient to repre-
‘sent the river valley. Second, the gross topography indicates no
sufficiently capacious valley leading toward Warsaw, and the ob-
‘Scuring drift is scanty. Third, while the Oatka has a handsome
‘valley from Warsaw to Pavilion this has neither the size, form nor
altitude that would represent the lower stretch of the river valley on
‘that meridian, in soft shales. Fourth, rock appears at Castile in
‘the bed of Wolf creek, at about 1260 feet altitude; and at the rail-
‘toad station rock underlies the surface at near 1400 feet, thus
effectua!ly closing any river escape in that direction. Fifth, the head
Of the Warsaw valley, at Rock Glen, is in rock on both sides of the
Valley axis, at 1200 and 1300 feet. Sixth, the Oatka valley quite
1 Bost. Soc. Nat. Hist. Proc. 1894. 26: 359-69.
74 NEW YORK STATE MUSEUM
disappears toward Leroy and the creek falls over the limestone in
a mere notch. Seventh, the Onondaga limestone has a practically
continuous outcrop from east of Batavia to the Genesee east of
Caledonia, and no heavy stream ever crossed its scarp in that region
in preglacial time. . : |
In attempting to locate the ancient valley for the interval from
Portage to Mount Morris we must apply the criteria as noted above
and use the principles and argument as in the Rochester district.
Assembling the topographic sheets it becomes apparent that only one
valley is found on the map which meets the conditions. The valley
of Nunda, now occupied by Keshequa! creek, and lying east of the -
present river, has fair direction, sufficient size and the proper depth
where unfilled. The extensive moraine between Portage and Oak-
land is evidently the barrier between the Portageville and Nunda sec-
tions of the great vallev. North and northeast of Portageville the
walls of the valley are only drift and no rock is found anywhere in ;
that district. On the steep slope south of Hunt (cut by the outflow |
of the fifth stage of the glacial waters as described below), in the -
creek gorge at Hunt’s Hollow, and on the slope northeast, the rocks
appear, but they mark only the eastern wall of the ancient valley. |
On the north no rock is found until the hill is reached north of
Oakland. The old valley is very wide here and was probably broad
ened by the junction of four streams: (1) the Genesee, passi g
northeast; (2) the Silver lake-Castile affluent, from the north.
west; (3) the St Helena tributary, from the north; and (4) the |
Dalton or upper Keshequa waters, from the southeast. This re |
lation is indicated in the accompanying map.
Downstream, or northeast of Nunda, toward Tuscarora
Sonyea the higher and broader cross-section of the old valley is very
satisfactory. From Nunda to Union Corners the eastern wall is
plainly the slope of a great valley. The western wall is equally
conspicuous though partially dissected by a shallow north and soutl
valley northwest of Tuscarora. From Tuscarora to Sonyea the bot
tom section of the old valley is obscured by drift and is not so ~
satisfactory. Rock appears at Sonyea station and half a mile east, ©
on the 600 feet contour, and in the 214 miles of the creek canyon |
south of Sonyea. Rock also appears north and south of Tuscaror
but probably leaves a channel a mile wide.”
Sa a
1See footnote on page 53.
2Mr. Charles Hageardorn of Tuscarora, who has bored many wells in the Nunda distric
informs the writer that borings at Nunda were in the drift to depth of 103, 97 and ’
feet. A mile east of Nunda Junction wells go to depths of 80 and roo feet witha
reaching rock; and in Tuscarora the drift is not less than 100 feet deep.
PLEISTOCENE HISTORY OF THE GENESEE VALLEY 75
The junction of the Genesee and Dansville valleys is not so clear
and satisfactory as we might expect. he rock exposures restrict
the valley width and the Genesee is made apparently a tributary to
the Dansville river. But this seems to be the only possible outlet.
It is probable that the preglacial Genesee river with its. full leagth
‘had not been in its acquired channel a great period of time, or in
‘other words was not a very ancient stream. The river had been
produced by the diversion or capture or union of different minor
streams, and had only in later time become adjusted to the course
‘in which the glacier found it. The Dansville river was probably
‘the older stream, though possibly smaller in volume. Before the
‘ice sheet interfered with it the Dansville river probably collected
pthe drainage from a large territory on the east of Dansville and
‘south of the western members of the Finger lakes, including the
“upper Cohocton valley. Some of this drainage was inherited from
‘the earliest time, and probably the valley had become mature while
‘the Genesee was young. The glacial drift cuts off the former upper
waters and sends them over southward by the Cohocton river, so
that the Dansville stream is today only the Canaseraga creek. The
‘greater maturity of the Dansville-Avon valley was noted by Dr
Grabau.
It must be noted that the present floor of the Dansville-Avon
palley is not the bottom of the old river valley, but only the top
‘of the deep filling left by the glacier and the glacial lakes, with
‘some contribution by the present streams.
Glacial waters and canyon cutting
_ The initiation of the postglacial canyons and the history of their
‘cutting is intimately tied in with the glacial lakes held in the valley.
The various benches along the new channels of the river and the
‘many terraces and plateaus of sand and gravel can not be under-
‘stood without a knowledge of the lake history of the valley. And
this drainage history of the Genesee valley is one of the most re-
markable and dramatic stories in geologic literature.
During the long time, to be counted as many thousands of years,
while the south edge of the ice sheet was slowly receding or backing
Naway, from south to north, across New York State, the waters
‘Over the Genesee area were held up to high levels, being force. to
Overflow east or west. In the successive lowering of the waters by
the opening of more northward outlets at least seven great
‘Tiver systems have received (and some of them more than once)
‘the contribution of Genesee waters. In order of time these are
| follows: (1) Pine creek-Susquehanna. (2) Allegheny-Ohto-
76 NEW YORK STATE MUSEUM
Mississippi. (3) Canisteo-Chemung-Susquehanna. (4) Glacial
lakes Warren and Chicago to Mississippi. (5) Mohawk-Hudson —
(6) Gilbert gulf (sea level waters in Ontario basin). (7) St~
Lawrence.
In the present knowledge of the glacial and postglacial history of
the Genesee drainage the writer recognizes at least 17 distinct stages”
or episodes. The first’ three stages involve onky “the upper”
(southern) part of the valley, the Portage district being then under
the glacier. The Portage-Mount Morris region is involved in the
history of stages 4 to 13. The subsequent stages concern only the
valley north of Mount Morris. The history will be given very con-
cisely in its relation to the district under present study. .
Stage 4. Belfast-Fillmore lake.! Outlet was at Cuba, to the
Allegheny-Ohio-Mississippi. Present altitude of outlet 1496 feet.
Present altitude of the lake plain on the Portage parallel about 1 530°
Feet. ; @
During this stage the ice front receded as far as Portage, and
lingering there deposited the Portage moraine which blocks the old.
valley in that district. South of Portage the valley was occupied by |
the lake which has left conspicuous evidences of its presence in the
many water-leveled plains and terraces in the upper valley, with —
deltas at the mouths of side streams, having elevations of 1500 feet |
and upward. |
Stage 5. Portage-Nunda lake. Outlet was by the Dalton-Swain
rock gorge to the Canisteo-Chemung-Susquehanna. Altitude of the |
channel head, at Rosses, 1320 feet. i
This stage endured while the ice front receded from Portage, |
Hunts and Dalton to Union Corners and Tuscarora, or through }
about 5 miles of meridional distance. However, the time involved |
was sufficient to allow the escaping waters to cut the steep rock |
bluffs south of Hunts and southeast of Dalton and the splendid |
rock gorge leading through Rosses and Swains to Canaseraga. As |
an example of an abandoned glacial river channel these features are |
unusually fine. = #
During this stage the Portage district was submerged in the lake -
waters which by their leveling action produced the level stretches |
and terraces of sand and gravel at and east of Portage with eleva
tion from 1300 to 1325 feet. The plain at the Erie Railroad viaduct
1325 feet, belongs in this category. The erosion plane of this lake
extends up the valley to Belfast, and being lower and nearer thé
1 A fuller description of these early stages is printed in Geol. Soc. Am. Bul. 7436-43. %
| PLEISTOCENE HISTORY OF THE GENESEE VALLEY Ta.
;
“middle of the valley they are the most conspicuous levels visible
from the railroad between Portageville and Belfast.
_ Stage 6. Dansville lake. Outlet was at Burns past Arkport and
-Horneli to the Canisteo-Chemung-Susquehanna. Present altitude of
‘the head of channel about 1210 feet. Present altitude of the lake
plane at Portage about 1230 feet.
_ The first cutting by the waters as they fell below the fifth stage
level is to be seen on the north point of the high ground in West
‘Sparta and about one mile southeast of Union Corners. Here was
‘the critical locality where the Portage lake waters first escaped be-
‘tween the receding ice wall on the north and the land slope on the
‘south. The notching on the nose of the hill is evident, though not
very conspicuous, at about 1300 feet and downward. When the
waters came to a standstill as the Dansville lake, they produced the
smoothing, leveling and shoreline work that is plainly seen at about
1200 feet around the nose of the hill.
_ This sixth stage lasted until the ice receded so as to uncover
‘ground below i2to feet in the vicinity of Linden and Attica, south
of Batavia. As this new escape is on a meridian so far away from
the Burns outlet no estimate of the duration of the waters can be
made based on distance of the ice front retreat. Undoubted terraces
of this level may be seen about Glen Iris at 1240 and higher; on the
delta of Wolf creek at 1220 to 1240; and a plateau east of Bishop
meormers and east of the river at 1230.
| Portageville morainal lake. With the fall of the glacial waters
below the Portage terraces, about 1320 feet, a local lake was left in
the valley above Portage, being hell up by the drift barrier. This
water we have called the Portageville morainal lake. It was con-
temporaneous with the sixth stage of the glacial waters (lying north-
ward), which from this time touch only the areas on the north.
It will now be seen that the gorge cutting at Portage began only
with the overflow of the Portageville morainal lake, and that the
glacial Dansville waters had no relation to the gorge except as pos-
sibly determining the base level for the stream and as the receiving
body for the detritus. The initiation of the gorge cutting probably
began at about 1320 feet, as it seems likely that the viaduct plain
originally extended entirely across the valley. The top of the rock
at the head of the canyon is at about 1240 to 1250 feet.
It will also be seen that the Portage river, draining the morainal
Take, could not cut its channel lower than about 1230 feet during the
life of the Dansville glacial waters, or only some to or 20 feet into
78 NEW YORK STATE MUSEUM
the rock. The stream detritus was dropped immediately northward
in the Dansville water, to be largely picked up in later stages of
the lowering waters and transported farther north.
The numerous lower terraces in the valley from Portageville up a
far as Caneadea, and ranging from 1270 down to Eye belong to the
morainal lake. 7
Stage 7. Mount Morris-Geneseo lake. Outlets were by a series
of channels on the meridian of Batavia and lying between Linden
and East Bethany. The flow was west, across the Oatka and
Tonawanda valleys to the great glacial lake Warren, with ultimate
escape by Chicago to the Mississippi. The elevation of the outlet .
channels declines from 1200 to 1000 feet. |
The former stages were comparatively steady levels of the waters,
with only slow lowering as a permanent outlet was downcut. But
this stage, and subsequent stages, comprise a series of falling water-
levels as the receding ice front pie lower and lower passes on the
north-facing slopes. .
The several terraces north of the tee falls, with elevations 0:
T1180, 1140 and 1090, may be correlated with these seventh s 3
waters. They represent remnants of the deltas built in the Mount
Morris-Geneso lake by the river while it was cutting the Portage
canyon. ,
Stage 8. Lake Hall. Outlets were between East Bethan
Batavia with elevations from 1000 down to goo feet, the wated
escaping to Lake Warren the same as in stage 7. !
So far as direction of escape is concerned this stage is only ;
continuation of the stage 7, the outlet channels forming a con
tinuous series [see N. Y. State Mus. Bul. 106, pl. 6]. It is made:
separate stage because the Genesee glacial waters are now blende
with the glacial waters of central New York. This stage is th
successor in the central part of the State to the glacial lake New
berry, which had its outlet south by Horseheads and Elmira to tt
Susquehanna. This body of water is named after James Hall. —~
The water-leveled areas which correlate with this stage are the |
terraces east of Bishop Corners, at 940, 900 and 860 feet; and fl
extensive delta plain at Nunda, declining from 940 to 860 feet.
Also the broad summit plateau at goo feet at the top of of Mot 1
Morris canyon, the “ High Banks.”
Stage 9. Lake Vanuxem. Outlets were at Syracuse to’
Mohawk-Hudson, at elevation of 900 feet and declining. ©
”
PLEISTOCENE HISTORY OF THE GENESEE VALLEY 70
4
; _ While the ice was resting against the salient at Batavia it receded
from the hills south and west of Syracuse permitting the impounded
| glacial waters to escape eastward, a direction of outflow contrary to
the former stage. The waters are named for Lardner Vanuxem,
“whose district in the early Geological Survey of New York com-
prised the central portion of the State.
| The higher terraces on the delta either side of the canyon at
~Mcunt Morris, at 840, 800 and 740, may have been made during
| this stage; also the deposits about the mouth of the Keshequa, and
the lower terraces east of Bishop Corners, at 825 and 750.
St Helena-Gibsonville morainal lake. When the waters fell
| below goo feet on the Mount Morris parallel the valley above the |
“High Banks” was left holding a local lake, which we name as
given above. In preglacial time this valley probably opened to the
south [see p. 73] as the walls at the north are rock. The lake may
be called morainal, however, since the south end was blocked by the
Portage moraine.
The St Helena-Gibsonville morainal lake (or St Helena lake for
brevity) was contemporaneous with the Lake Vanuxem and later
‘waters. The initial height of the lake is definitely shown by the
broad gravel plain, coinciding with the top of the rock, at the “ High
Banks” at goo feet; and the extensive delta plateau opposite the
Silver lake outlet also at goo feet. All terraces in the St Helena
Valley below goo feet must belong to the local lake and correlate
with the downcutting of the Mount Morris canyon.
As the crest of the lower Portage falls is only 850 feet in altitude
they could not have been initiated until the “ High Banks” outlet
and St. Helena lake was lowered to that level.
Tuscarora morainal lake. With the falling of the waters in the
‘Dansville valley below 800 feet a local morainal lake was left in
the lower or northern part of the Nunda valley, due to the drift
blockade south of Sonyea. This local water did not reach as far as
Nunda but covered the site of Tuscarora.
The point of lowest escape was north of the moraine, and north
of the ancient valley. Falling on the rock the outlet was compelled
to cut the shallow canyon, about 100 feet deep, southwest of Sonyea
now occupied by the Keshequa creek and utilized by the railroad,
During stages 9 to 12 the cutting must have proceeded, but with
‘interruptions as the base level waters in the Dansville valley changed
their level.
80 NEW YORK STATE MUSEUM
Stage 10. Avon lake. Outlets were at Honeoye Falls, Rush and |
Mendon, at 700 down to 580 feet, eastward to the Mohawk-Hudson,
Following the Vanuxem stage the ice at Syracuse receded so as
to allow free river-flow through the site of that city and there was
no extensive lake then held in central New York. But in the
Genesee Valley the ice lay so far to the south that a local lake was
held in the valley with its levels determined by the outlets noted
above. The highest of these channels lies 2 miles west of Honeoye
Falls and the lowest is the excellent abandoned channel followed by |
the Lehigh Valley Railroad through Rush to Mendon, at 580 feet. :
This Avon lake flooded the Dansville valley.
Stage 11. Second Lake Vanuxem. The relationship of phe
nomena in the Genesee and Batavia region theoretically requires aa
readvance of the ice at Syracuse and the restoration of the glacial
Lake Vanuxem.'. . -
It is not determined to het height the second Vanuxem rose, __
but it may have reached an altitude approaching 840 feet on the ©
Mount Morris parallel. While this water lay over the Genesee
region the ice backed away from the Batavia salient sufficient to
allow Lake Warren to spread in from the west, and we have
Stage 12. a
Stage 12. Lake Warren. Outlet was across the State of Michi-
gan into the glacial lake Chicago and out to the Mississippi. Alti-
tudes of the Warren beaches are generally about 880 feet in central
New York, but on the Mount Morris parallel the plane is about
840 feet. 3
Stage 13. Lake Dana. Outlet was eastward toward the
Mohawk-Hudson, at elevation about 700 feet, or about 660 feet on
the Mount Morris parallel. q
Lake Dana was only the longest of the pauses in the lowering of
the Warren waters toward the Iroquois level. It is one phase of the
Hyper-Iroquois waters.
The filling of the Genesee valley from Dansville to Scottsvill
with lake silts and smoothing them to the present form has beer
a process in activity since the sixth stage, and is now carried on by |
the present streams.
1 The discussion of the glacial lake history of central New York and descripiiaa of
the drainage channels and lake phenomena will be found in a forthcoming bulletin ¢
the State Museum. a
PLEISTOCENE HISTORY OF THE GENESEE VALLEY SI
Later stages
- Other stages now recognized are those of the Scottsville lake;
Lake Iroquois; Gilbert gulf (sea level waters) ; and Lake Ontario.
As water planes they lie inferior to the valley bottom at Mount
Morris and therefore do not properly appear in this connection.
Epitome of the history
Stage 4 Belfast-Fillmore lake. Outlet at Cuba; 1496 feet. Port-
age moraine formed. ,
Stage 5 Portage-Nunda lake. Outlet at Swains; 1320 feet. Erie
Pe =» viaduct terraces formed.
ftaze 6 Dansville lake. Outlet at Burns; 1210 feet. -Portage-
él ville morainal lake and beginning of the Portage
canyon. WDelta terraces at Glen Iris and mouth of
| Wolf creek.
Stage 7 Mount Morris-Geneseo lake. Outlets at Linden-Beth-
aes any; 1200-1000 feet. Delta terraces about the lower
falls.
setaoe o@ ake Hall. Outlets at Batavia; 1000-900 feet. Ter-
; races east of Bishop Corners; Nunda plain.
Stage 9 Lake Vanuxem. Outlets at Syracuse; 900 and declin-
ing. St Helena-Gibsonville morainal lake and _ be-
ginning of the “ High Banks” canyon. Tuscarora
morainal lake and beginning of the Sonyea ravine.
_ Upper terraces on Mount Morris delta.
Stage 10 Avon lake. Outlets at Honeoye Falls-Rush; 700-580
feet. Filling in Dansville-Avon valley.
Stage 11 Second Lake Vanuxem. Outlets at Syracuse; 700 feet
and rising.
Stage 12 Lake Warren. Outlet via Chicago to Mississippi; about
A 840 feet on the Mount Morris parallel.
Stage 13. Lake Dana. Qutlet toward the Mohawk-Hudson; about
660 feet on the Mount Morris parallel.
Canyons and cataracts
The Portage canyon was cut by the outflow of the morainal lake
held in the valley above Portageville, the earlier flow being into the
glacial waters of stages 6-8, described above, and the later flow
into the St Helena morainal lake.
The ravine and cataracts were not produced by free and uninter-
rupted flow of the river, with deepening of the whole ravine from
ee See we
82 NEW YORK STATE MUSEUM
north to south, or upstream. The cutting of the canyon progressed
downward from the top and from south to north. The upper
cataract was established first and independently before the lower or —
deeper portion of the canyon had any existence. The down cutting
of the canyon proceeded only as the receiving waters (stages 6-8)
were lowered. The quantitative or progressive relationship of the
two factors is uncertain, but it is quite possible that the glacial
waters were so long-lived that the canyon cutting kept pace with or
were even limited by the falling baselevel waters.
This relation of river and lakes explains the existence of three
cataracts instead of only one, as would probably have been the case
if the river could have fallen freely through the whole distance from
Portageville to St Helena and the canyon cutting could have pro-
geressed normally and without vertical limitation. In rocks of
variable hardness or resistance a stream might alone develop multiple
cataracts, but the variation of the strata in the Portage section is
not sufficient to cause three cataracts with the spacing that now
exists.
When the Portageville morainal lake came into independent ex-
istence by the fall of the broader glacial waters below the level of the
Erie Railroad viaduct plain, stream outflow began, probably at about
the position of the railroad viaduct. The fall of the stream, how-
ever, was limited by the level of the receiving waters, and during
the long life of the Dansville and Mount Morris-Geneseo lakes
(stages 6 and 7) the river work was restricted to the higher part of
the canyon. The lower part of the canyon, including the middle
and lower contracts, did not then exist, being covered and pro-
tected by the lake waters. The upper and south cataract was in-
dependentiy initiated and established, and probably receded some
distance, before the lower and northern part of the gorge had any
existence. Eventually the falling of the glacial waters through the
stages 6 and 7 brought the river into play in the horizon of the
middle cataract.
As the crest of the third and youngest cataract is only about 850 _
feet elevation it is below the top of the High Banks canyon at Mount |
Morris, and it is therefore evident that the lowest part of the |
Portage canyon and the lowest cataract came into existence only *
the High Banks was cut.
On account of the changes which have been produced subsequent
to the initiation of the cataracts and the withdrawl of the glacia
PLEISTOCENE HISTORY OF THE GENESEE VALLEY 83
waters it is not possible to correlate with precision the production of
_ the cataracts and the limiting lake waters. The upper cataract
correlates with the Mount Morris-Geneseo lake, though the begin-
ning of the canyon was during the life of the Dansville lake. The
middle cataract, with a crest altitude of 1005 feet, seems to belong
with the Lake Hall stage. The lower cataract correlates with Lake
_ Vanuxem and later stages. The initiation of the Portage canyon
Was an interrupted process, covering a varied lake history and a
long period of time.
The Mount Morris or High Banks canyon is in shales of such
weakness and uniformity that probably no large cataract was ever
produced. The river rapidly removed all obstructions to its flow
and acquired a uniform or graded slope. The initiation of the gorge
was probably during the closing phase of Lake Hall, and the gorge
may have been entirely cut during the life of the first Lake Va-
nuxem and the Avon lake. The gorge was cut from the top down-
ward, and probably the erosion kept pace with the fall of the waters
in the Dansville valley. If the strata were as hard as the Portage
rocks probably cataracts would occur here also.
The history of the Rochester canyon is similar to that of the
Portage. The upper cataract was established during the life of
Lake Iroquois, the plane of which was nearly 200 feet above that
of Lake Ontario. With the falling away of the Iroquois waters the
lower and northern part of the gorge, with the middle and lower
cataracts, came into existence.
Deformation of the lake planes
In making close correlation of the lake phenomena and drainage
it is necessary to take into the account the warping or tilting of
the land which has occurred since the glacial time, and the conse-
quent rise to northward which has been given to all the planes of the
ancient lakes. The amount of deformation of the Portage-Mount
Morris district is not known with precision but probably it is not
far from 2 feet per mile.
The difference in the height of the correlating features according
to latitude has not been regarded in the above description, except
in a few cases. The figures used in the description are the altitudes
which the features have as they stand today. In order to find the
correlating planes for localities of different latitude 2 feet per
mile should be added for northing or substracting for southing.'
1 Some discussion of the matter of deformation of the lake planes is given in N. Y
State Mus. Bul. 106, p. 76-79.
84 -- - NEW YORK STATE MUSEUM
For close correlation of the lake-level features some allowance
should be made for the depth of water in the outlet channel, and for
the down cutting of the outlet during the life of the lake.
Detrital filling of the valleys
All the ancient valleys have been so filled with glacial drift and 4
lake sediments that in the absence of borings the grade slopes of
the streams can not be determined. The localities of diverted drain-
age have been blocked by morainal drift, while the more open
stretches of the valleys are,more or less filled with stream detritus —
and Jake silts, which may overlie glacial deposits.
The old valley above Portage has been considerably filled with q
glacial rubbish and later by lake Sainer i during the lacustrine q
stages 4 and 5.
The St Helena valley was largely filled with delta stuff during the 7
stages 6 to 8, and during the life of the St Helena-Gibsonville mor- —
ai fi = Si
——— mF .
=_——
a a i A
ainal lake. With the cutting down of the “ High Banks” it has been —
reexcavated. Any flooding during the stages 11 to 13 that over- —
topped the outlet stream must have produced deposition with sub-_
sequent reexcavation.
The Nunda valley was subject to re deposition during the stages”
6 to 9, and stages 11 and 12.
The old and broad valley from Dansville to Avon has evidently
been subject to lake filling during all the stages from 6 to I 3 and
stream aggradation is still active.
5
eh
z
Yr |
_
INDEX
Acanthodus pristis, 56.
Ambocoelia, 60.
.umbonata, 68.
American Bluestone Co., 61.
Atrypa aspera, 68.
Aulopora, 62.
annectens, 5I, 54.
Avon lake, 80, 81.
Bactrites aciculum, 50, 52, 54, 60.
Belfast quadrangle, 68.
Belfast-Fillmore lake, 76, 81.
Bibliography, 44-45.
Bluestone, rock exposures at, 65.
Bluestone quarries, 61.
Buchiola lupina, 61.
ememsestriata, 51, 52, 54, 50, Or, 66,
speciosa, 57.
Buck run ravine, 53, 55, 56, 57.
Byersville, rock exposures near, 50,
62.
Camarotoechia sp., 68.
Canaseraga valley, 55, 57, 59.
Caneadea creek, 68.
Canyons, 81-83.
Cashaqua creek, 55, 56, 57, 59.
Cashaqua shale, 46, 47, 48, 49, 53-
2755, 65.
Castile, rock exposures near, 62,
Catatacts, 81-83.
Catlin, rock exposures at, 67.
Chemung fauna, 62.
Chemung group, 66-68.
Chemung sandstones and shales,
46, 48.
Chonetes, 60.
Cladochonus, 61.
Clarke, John M., cited, 45, 50, 52,
53, 54, 55, 64.
Classification, 46-47.
Crinoid stems, 62.
Dalton, rock exposures near, 65.
Dana, Lake, 80, 81.
Dansville and Genesee
junction of, 75.
Dansville lake, 77, 81.
Detrital filling of the valleys, 84.
Dip, 68-60.
valleys,
East Koy creek, 67.
Entomis serratostriata, 60.
variostriata, 60.
Brey cake, 54.55. 62.
Erin, rock exposures at, 67.
Euthydesma subtextile, 61.
Fairchild, Herman L., Pleistocene
History of the Genesee Valley
in the Portage District, 70-84.
Fall brook ravine, 49, 50, 51, 52, 59.
Fillmore; rock exposures near, 65.
Flume, 60.
Formations, description of, 47-609.
Fucoides graphica, 57, 61.
verticalis, 46, 61, 62.
Gardeau flags and shale, 47, 48, 58-
Or, 62:
Gardeau Flats, 56, 57.
Gardeau group, 46, 55.
Genesee Falls, 47.
Genesee river gorge, 47, 61; diver-
sions, 7I-75.
Genesee shale, 46, 48-50, 68.
Genesee valley, 65; in the Portage
district, pleistocene history, by
Herman L. Fairchild, 70-84;
junction with Dansville valley,
75:
86
Genesee Valley Bluestone Co., 61.
Geneseo, rock exposures at, 49, 50,
SI.
Genundewa limestone, 48, 49, 50-
BT:
Gephyroceras en SI.
Gibson’s glen, rock exposures at,
59, 60.
Gibsonville, rock exposures at, 55,
50, 57
Gilbert gulf, 81.
Glacial waters and canyon cutting,
75-80.
Gorham, rock exposures at, 50.
Grabau, cited, 73.
Greigsville, rock exposures near,
BT.
Grimes sandstone, 48, 57-58.
Griswold, rock exposures at, 51.
Groveland station, rock exposures
near, 55, 56, 58, 59.
Haggardorn, Charles, cited, 74.
Hall, James, cited, 44, 46, 48, 40,
50, 63-64, 65, 67.
Fall, . Lake, 78; 81,
Hatch flags and shale, 48, 56-57.
High Banks, rock exposures at, 54,
56.
High Banks canyon, 83.
High Point sandstone, 62, 63.
Hogsback,. 53,°55; 56.
Honeoyea desmata, 61.
erinacea, €0.
major,” 54,0%:
styliophila, 51.
Horsford, Eben N., cited, 45.
Hunt, rock exposures near, 65.
Hyolithus neapolis, 66.
Irondequoit valley, 72.
Iroquois, Lake, 81.
Ithaca beds, 57.
'Lake planes, deformation, 83-84.
Lamont, rock exposures near, 67.
Leptostrophia, 60.
Letchworth, William Pryor, 44.
NEW YORK STATE MUSEUM
LL
Melocrinus clarkei,
Letchworth Park, 44.
Lignites, 61.
Lingula ligea, 52, 54, 56, 66.
cf. melie, 68.
spatulata, 50,.§2:
Liorhynchus multicosta, 68.
quadricostatus, 50.
Little Beards creek, 40.
Livingston county, 51.
Long Beards Riffs sandstone, 65;
07.
Lower black iia 53.
Lower Fucoidal group, 46.
Lower Portage fall, 60.
Loxonema muitiphcatum, 60. 4
Lunulicardium (Pinnopsis) acuti- —
rostrum, 54.
bickense, 60.
_ (Pinnopsis) ornatum, de
_ (Pinnopsis) wiscoyense, 66.
Luther, D.D., cited, 45, 50, 52, 64, —
65. a
Manticoceras intumescens zone, 51. }
oxy, 60, 62, 66.
pattersoni, 54, 57, €o.
var. styliophilum, 51.
rhynchostoma, 60, 62, 66.
Marsh, O. C., mentioned, 45.
51, 54.
Middlesex shale, 48, 52-53.
Mill’s Mills, rock exposures at, 67.
Moscow, rock exposures at, 49, 50, —
eee *
Moscow shales, 68.
Mount Morris, rock exposures at,
48, 49, 50, 53, 56, 57.
Mount Morris canyon, 83.
Mount Morris-Geneseo lake, 78, sr.
Murder creek, 51.
0 ee
Naples, rock exposures at, 55, 57 a
58. _
Naples fauna, 51, 57. -
Naples valley, 57. “
North Evans, rock exposures at,
53.
NEW YORK STATE MUSEUM
Nunda, rock exposures at, 60, 62,
65.
Nunda group, 46;
name, 47. git a
Nunda sandstone, 47, 48, 61-64.
- Nunda valley, 50, 74.
introduction of
- Oatka creek valley, 50, 65, 73.
™ Ontario accincta, 54.
clarkei, 61.
suborbicularis, 54, 57, 61.
» Ontario county, 51.
Ontario depression, 70.
_ Ontario, Lake, 81.
_ .Orbiculoidea sp., 62.
= alleshania, 68.
lodensis, 50, 52.
cf. media, 68.
Orthoceras sp., 66.
filosum, 54.
ontario, 54.
Nacator,54; 57, 60.
Palaeoneilo petila, 54.
Palaeotrochus praecursor, 57, 60.
Paleoniscus devonicus, 56.
Paracardium doris, 54, 61, 66.
‘Parrish limestone, 54.
Penn Yan, rock exposures at, 53.
Perry, rock exposures near, 58.
Puiraszmostoma natator; 51, 54, 57,
60.
Pike, rock exposures near, 67.
‘Pike creek, 52, 53.
Pinnopsis see Lunulicardium.
Pleistocene history of the Genesee
valley in the Portage district, by
Herman L. Fairchild, 70-84.
Pleurotomaria sp., 66.
rugulata, 50, 52.
Polygnathus dubius, 56.
Portage canyon, 81.
Portage group, 46, 57, 63; first use
as a group term, 46; use of term,
47.
Portage-Mount Morris district, 73-
75:
Portage-Nunda lake, 76-77, 81.
—eeeeEeEeeeeeeeeeeeeeeeeeEeeoeeeeeeeeeeeeeeeeeeeEeEeeEeEeEeeEeeeeeeEeeeeeeeeeeeeeeeeeeeeeeeeeeeeEeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeeee eee ee
87
Portage shales and sandstones, 46,
47.
Portageville, rock exposures at, 61,
2, 65:
Portageville Bluestone Co., 61.
Portageville morainal lake, 77-78.
FPosidomiavattica,/Or,
Powell, Maj. John W., mentioned,
AGS
Prioniodus erraticus, 56.
spicatus, 56.
Pristacanthus vetustus, 56.
Probeloceras lutheri, 50, 54, 57.
| Productella hirsuta, 68.
lachrymosa, 68.
speciosa, 68.
Pterochaenia cashaqua, 54.
ifasilis. 50, 51, 52, 54,02.
Quarry hill, rock exposures at, 60,
62.
Relyea creek, 62, 65.
Rhinestreet black shale, 48, 54, 55-
56.
Rochester district, 72-73, 83.
Rock Glen, rock exposures at, 62.
St Helena bridge, 56, 57.
St Helena creek, 73.
St Helena Flats, 56.
St Helena-Gibsonville morainal lake,
79.
Scottsville lake, 81.
Seneca county, 53.
Seneca lake, 53.
Silver lake outlet, 57, 58.
Smoky Hollow, rock exposures
near, 54, 58.
Sonyea, rock exposures near, 53,
55, 56.
South Warsaw, rock exposures
near, 59.
Spathiocaris emersoni, 56.
Spirifer disjunctus, 63, 66, 68.
mesacostalis, 68.
Springwater valley, 57.
Standish shale, 52.
Steuben county, 65.
88
Stony creek, 59, 62, 65.
Styliola band, 50.
Styliolina fissurella, 50, 51, 60.
Table rock, 47, 58, 59, 60.
Tompkins county, 57.
Tornoceras uniangulare, 51, 54, 60.
Tuscarora, rock exposures at, 56,
57:
Tuscarora morainal lake, 79.
Upper black shale, 48, 49.
Upper falls, 58.
Upper Fucoidal group, 46.
Upper Genesee beds, 49.
Vanuxem, Lake, 78-79, 81; second,
80, 81.
Veteran, rock exposures at, 67.
Warren, Lake, 80, 81.
NEW YORK STATE MUSEUM
a rock exposures near, 62,
ce Bluestone Co., 61.
Warsaw valley, 50.
Warsaw-Wyoming valley, 73.
West River shale, 48, 51-52.
West Sparta, rock exposures near,
"57, 58, 59.
Wildcat gully, 59, 62.
Williams; H. S.seltediaas
Wiscoy, rock exposures at, 64, 65,
68.
Wiscoy falls, 65°67:
Wiscoy shales and sands, 48, 64-
66.
Wolf creek, 56, 57, 58, 62.
Yates canny 52.553.
Zaphrentis sp., 66.
ee ee ee
a i ee:
Se eee
- New York State Education Department
‘New York State Museum
Joun M. Crarxe, Director
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Geology. Gz (14) Kemp, J. F. Geology of Moriah and Westport Town-
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decheologs” oat Art (16) Beauchamp, W.M. Aboriginal Chipped Stone Im-
plements of New York. 86p. 23pl. Oct. 1897. 25¢.
Ar2 (18) Polished Stone Articles used by the New York Aborigines.
to4p. 35pl. Nov. 1897. 25¢.
Ar3 (22) —— Earthenware of the New York Aborigines. 78p. 33pl. Oct.
1898. 25¢.
NEW YORK STATE EDUCATION DEPARTMENT
Ar4 (32) Aboriginal Occupation of New York. -190p. 16pl. 2 maps.
Mar. 1900... g6¢-
Ars (41) Wampum and Shell Articles used by New York Indians.
166p. 28pl. Mar. 1901. 306.
Al tle ab shee a teckel
Ar6 (50) Horn and Bone Implements of the New York Indians. 112.
43pl. Mar. 1902. 306.
Ary (55) —— Metallic Implements of the New York Indians. 94p. 38pl.
June 1902. 25¢.
Ar8 (73) Metallic Ornaments of the New York Indians. 122p. 37pl.
Dec. 1903. 306. 2
Arg (78) History of the New York Iroquois. 340p. 17pl. map. Feb. —
r905. 9756, cloth.
:
Arto (87) Perch Lake Mounds. 84p. ta2pl. Ap. 1905. 20¢. 4
aad a —— Aboriginal Use of Wood in New York. 1go0p. 35pl. June
oe.
Bera oR) —— Aboriginal Place Names of New York. 336p. May 1907. ©
406.
Ar 13 (113) —--- Civil, Religious and Mourning Councils and Ceremonies of ~
Adoption. 118p. 7pl. June 1907. ge5e. é
Ar 14 (117) Parker, A. C. An Erie Indian Village and Burial Site. 102p.. a
48pt. iv Dec.. r9e7- 3086:
Miscellaneous. Msr (62) Merrill, F. J. H. Directory of Natural —
Museums in United States and Canada. 2 36p-: Ap. 1008; 4 gan
Ms2 (66) Ellis, Mary. Index to Publications of the New York State Nat- _
ural History Survey and New York State Museum 1837-1902. baa ‘
June 1903. 75¢, cloth. ‘
Museum memoirs 1889—date. Q.
1 Beecher, C. E. & Clarke, J. M. Deyslawarear of Some Silurian Brachi- ©
opoda. 96p. 8pl. Oct. 1889. $1.
2 Hall, Tacs & Clarke, J. M. Paleozoic Reticulate Gnoneeel 350p. il. zopl.
1898. $1, cloth.
3 Clarke, J. M. The Oriskany Fauna of Becraft Mountain, Columbia Co.
N. ¥.°128p:. opl. --Oectreons “sag
4 Peck,C.H. N. Y. Edible Fungi, 1895-99. 106p.2s5pl. Nov.1900. 756,
This includes revised descriptions and illustrations of fungi reported in the 49th, 51st and ~
52d reports of the State Botanist.
5 Clarke, J. M. & Ruedemann, Rudolf. Guelph Formation and Fauna of
4d New York State. r1o96p. arpl. July 1903. $1.50, cloth. f
6 Clarke, ee Naples Fauna in Western New York. 268p. 26pl. map. —
$2, clot
7 Ruedemann, Rudolf. Graptolites of New York. Pt 1 Graptolites of the —
Lower Beds. 350p.17pl. Feb. 1905. $1.50, cloth.
8 Felt, E. P. Insects Affecting Park and Woodland Trees. v.1 460p.
il. 48pl. Feb. 1906. $2.50, cloth. v.2 548p. il. 22pl. Reb. sagegem
$2, cloth.
g Clarke, J. M. Early Devonic of New York and Eastern North America.
In press.
to Eastman, C. R. The Devonic Fishes of the New York Formations.
236p. rspl. 1907. $1.25, cloth. 4
Eaton, E. H. Birds of New York. In preparation.
Ruedemann, R. Graptolites of New York. Pt 2 Graptolites of the Higher
Beds. In press
Natural history of New York. 3ov. iJ. pl. maps. Q. Albany 1842-94.
DIVISION 1 ZOOLOGY. De Kay, James E. Zoology of New York; or, The
New York Fauna; comprising detailed descriptions of all the animals”
hitherto observed within the State of New York with brief notices of
those occasionally found near its borders, and accompanied by appropri-
ate illustrations. 5v.il.pl.maps. sq.Q. Albany 1842-44. Out oj print.
Historical introduction to the series by Gov. W. H. Seward. 178p.
v. 1 ptr Mammalia. 131+46p. 33pl. 1842.
300 copies with hand-colored plates.
v. 2 pt2 Birds. 12+380p. r41pl. 1844.
Colored plates. ;
v. 3 pt3 Reptiles and Amphibia. 7+ 98p. ptq Fishes. 15+415p. 1842.
pt3-4 bound together.
v. 4 Plates to accompany v. 3. Reptiles and Amphibia 23pl. Fishes 7gpl.
1842. Pea
300 copies with hand-colored plates.
a
—e ape
MUSEUM PUBLICATIONS
v. 5 pts Mollusca. 4+271p. 4opl. pt6 Crustacea. yop. 13pl. 1843-44.
Hand-colored*plates; pts5—6 bound together.
DIVISION 2 BOTANY. ‘Torrey, John. Flora of the State of New York; com-
prising full descriptions of all the indigenous and naturalized plants hith-
erto discovered in the State, with remarks on their economical and medical
properties. 2v.il. pl.sq.Q. Albany 1843. Out of print.
v. t Flora of the State of New York. 12+484p. 72pl. 1843.
300 copies with hand-colored plates. ,
W. 2 Plora of the State of New York. 572p. 89pl. 1843.
300 copies with hand-colored plates.
DIVISION 3 MINERALOGY. Beck, Lewis C. Mineralogy of New York; com-
prising detailed descriptions of the minerals hitherto found in the State
of New York, and notices of their uses in the arts and agriculture. il. pl.
sq.Q. Albany 1842. Out of print.
v. 1 ptr Economical Mineralogy. ptz Descriptive Mineralogy. 24+536p.
1842.
8 plates additional to those printed as part of the text.
DIVISION 4 GEOLOGY. Mather, W. W.; Emmons, Ebenezer; Vanuxem, Lard-
ner oe Hall; James. Geology of New York. gv. il. pl. sq. O. Albany
1842-43. Out of print.
v. 1 ptr Mather, W. W. First Geological District. 37+653p. 46pl. 1843.
v 2 pt2 Emmons, Ebenezer. Second Geological District. 10+437p. 17pl.
1842.
_v. 3 pt3 Vanuxem, Lardner. Third Geological District. 306p. 1842.
v. 4 pt4 Hall, James. Fourth Geological District. 22+683p. 1opl. map.
1843.
DIVISION 5 AGRICULTURE. Emmons, Ebenezer. Agriculture of New York;
comprising an account of the classification, composition and distribution
of the soils and rocks and the natural waters of the different geological
formations, together with a condensed view of the meteorology and agri-
ee. productions of the State. 5v.il.pl.sq.Q. Albany 1846-54. Out
of print.
v. 1 Soils of the State, their Composition and Distribution. 11 +371p. 21pl.
1846.
v. 2 Analysis of Soils, Plants, Cereals, etc. 8+343+46p. 42pl. 1849.
With hand-colored plates.
v.34 Eruits, etc.’ 8+340p. 1851.
v. 4 Plates to accompany v. 3. ogspl. 1851.
.Hand-colored.
v. 5 Insects Injurious to Agriculture. 8+272p. 5opl. 1854.
With hand-colored plates.
DIVISION 6 PALEONTOLOGY. Hall, James. Palaeontology of New York. 8v.
il. pl. sq. Q. Albany 1847-94. Bound in cloth.
v. 1 Organic Remains of the Lower Division of the New York System.
23+338p. gopl. 1847. Out of print.
v. 2 Organic Remains of Lower Middle Division of the New York System.
8+362p. 10o4pl. 1852. Out of print.
v. 3 Organic Remains of the Lower Helderberg Group and the Oriskany
Sandstone. pti, text. 12+532p. 1859. [$3.50]
pt2. 143pl. 1861. [$2.50]
v. 4 Fossil Brachiopoda of the Upper Helderberg, Hamilton, Portage and
Chemung Groups. 11+1+428p. 6o9pl. 1867. $2.50.
v. 5 ptr Lamellibranchiata 1. Monomyaria of the Upper Helderberg,
Hamilton and Chemung Groups. 18+268p. 45pl. 1884. $2.50.
Lamellibranchiata 2. Dimyaria of the Upper Helderberg, Ham-
ilton, Portage and Chemung Groups. 62+293p. 5ipl. 1885. $2.50.
pt2 Gasteropoda, Pteropoda and Cephalopoda of the Upper Helder-
berg, Hamilton, Portage and Chemung Groups. 2v. 1879. v. 1, text.
15 +4092p. v. 2, r20pl.. $2.50 for 2 v.
& Simpson, George B. v. 6 Corals and Bryozoa of the Lower and Up-
per Helderberg and Hamilton Groups. 24+298p. 67pl. 1887. $2.50.
& Clarke, John M. v. 7 Trilobites and other Crustacea of the Oris-
kany, Upper Helderberg, Hamilton, Portage, Chemung and Catskill
Groups. 64+236p. 46pl. 1888. Cont. supplement to v. 5, pt2. Ptero-
poda, Cephalopoda and Annelida. 4g2p. 18pl. 1888. $2.50.
as
NEW YORK STATE EDUCATION DEPARTMENT hee |
& Clarke, John M. v. 8 ptr Introduction to the Study of the General
of the Paleozoic Brachiopoda. 16+367p. 44pl. 1892. $2.50.
& Clarke, John M. v.8ptz Paleozoic Brachiopoda. 16 +394p. cap
1894. $2.50.
Gutadonie of ‘the Cabinet of Natural History of the State of New York a
2 cai Historical and Antiquarian Collection annexed thereto. 242p. Oo.
ae ae 1893—date.
In quantities, 1 cent for each 16 pages or less. Single copies postpaid as below.
New York State Museum. 52p.il. 4c.
Outlines history and work of the museum ‘with list of staff 1902.
Paleontology. 12p. 2¢.
Brief outline of State Museum work in paleontology under heads: Definition; Relation t
biology; Relation to stratigraphy; History of paleontology in New York.
Guide to Excursions in the Fossiliferous Rocks of New York. tr24p. 8c.
Itineraries of 32 trips covering nearly the entire series of Paleozoic rocks, prepared specially
for the use of teachers and students desiring to acquaint themselves more i > with the e
classic rocks of this State.
Entomology. 16p. 2¢. a
Economic Geology. 44p. 4c. | . <a
Insecticides and Fungicides. 20p. 3¢. ae
Classification of New York Series of Geologic Formations. ie Eisen a
Geologic maps. Merrill, F. J. H. Economic and Geologic Map of the State
of New York; issued as part of Museum bulletin 15 and 48th Museum
Report, v. 1. 59x67.cm. 1894. Scale 14 miles to 1 inch. 1§c. es
Map of the State of New York Showing the Location of Quarries | of
Stone Used for Building and Road Metal. Mus. bul. 17. ae LOC. = am
Map of the State of New York Showing the Distribution of the Rock —
Most Useful for Road Metal. Mus. bul. 17. 1897. 5c. + Sg 4
Geologic Map of New York. 1901. Scale 5 miles to 1 inch. - In atlas
form $3; mounted on rollers $5. Lower Hudson sheet 6oc. ae
The lower Hudson sheet, geologically colored, comprises Rockland; Orange, Dutchess, Put-
nam, Westchester, New York, Richmond, Kings, Queens and Nassau counties and parts 0
Sullivan, Ulster and Suffolk counties; also northeastern New Jersey and part of wes tern
Connecticut. 4
Map of New York Showing the Suriace Configuration and Water She eds.
t901. Scale x2 miles to 1 inch. + 156; a
Map of the State of New York Showing the Location of its Boos m nic
Deposits. 31904. Scale 12 miles to 1 inch. 15¢. i.
Geologic maps on the United States Geological Survey topographic ft ase}
scale 1 in. == 1m. Those marked with an asterisk have also een pub-
lished separately. 7a
*Albany county. Mus. rep’t 49, v. 2. 1898. 506. <=
Area around Lake Placid. Mus. bul. 21. 1808. oon
pcs of Frankfort Hill [parts of Hertnnes and Oneida counties]. Mt
t ET, V. 3. 1859.
Roc: land county. State geol. rep’t 18. 1899.
Amsterdam quadrangle. Mus. bul. 34. 1900.
*Parts of Albany and Rensselaer counties. Mus. bul. 42. 1901. roc.
*Niagara river. Mus. bul. 45. igor. 25¢.
Part of Clinton county. State geol. rep’t ro. or.
oe Bay and Hempstead quadrangles on Lore Island. Mus. bul.
190
Burtions of Clinton and Essex counties. Mus. bul. 52. 1902. . 4
Part of town of Northumberland, Saratoga co. State geol. rep’t 21. 1903.
Union Springs, Cayuga county and ostean baba bul. 69. 1903. -
*Olean quadrangle. Mus. bul. 69. 1903. i
*Becraft Mt with 2 sheets of sections. (Scale. tin= 4m.) Mus. bail 69
‘ 1903. 206.
*Canandaigua-Naples quadrangles. Mus. bul. 63. 1904. 200.
*Little Falls quadrangle. Mus. bul. 77. 1905. 15¢.
*Watkins-Elmira quadrangles. Mus. bul. 81. 1905. 206.
*Tully quadrangle. Mus. bul. 82. ro905. toc.
*Salamanca Bs pomp Mus. bul. 80. 1905. roe. ;
*Buffalo quadrangle. Mus. bul. 99. 1906. ‘roc. oa
*Penn Yan-Hammondsport quadrangles. Mus. bul. ror. 1906. 206. .
*Rochester and Ontario Beach Quadrangles. Mus. bul. ‘II4. 206, e
*Long Lake Quadrangle. Mus. bul. 115. roc.
*Nunda-Portage Quadrangles. Mus, bul. 118. 20c,
4
BULLETIN. 116
NOA— PORT ACE AN =
77 45 yi
Geology by D. D. Luther. }
|
EDUCATION DEPARTMENT
JOuM M_CLARIC
STATE CEOLOGIST ae oe Es
STATE MUSEUM
BULLETIN 118
NUNDA-PORTAGE QUADRANGLES
LEGEND
is
‘
q OUR WMORRIS.
Geology by 0. D,
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NDA- PORTAGE QUADRANGLES
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EDUCATION DEPARTMENT
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; STATE MUSEUM
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Rock: Glen
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DIAGRAM SHOWING ROCK SECTION EXPOSED ON NUNDA AND PORTAGE
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EDUCATION DEPARTMENT
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STATE GEOLOGIST
Portageville
UNIVERSITY OF THE STATE OF NEW YORK
STATE MUSEUM
GEOLOGIC MAP
OF
LETCHWORTH PARK
BULLETIN 118
LEGEND
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