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aeece eee

: vpn :

Ls

Re the field aes
tions in the fie 1900-1 pie =, Sc
MER en. Ob. oro. a.---. 442

work. ec ee treet ret wese erm eet eee 442
orial tablet for the Emmons house 452

AOS eee eee 456

_ Locality record of specimens......-. 456

: eee Bancroft Simpson -.....---. 457
_ Appendix 1: Accessions

SS ee ere aera 461

memmnianes oS... 2: 5... 463

: Pere iatises ee con. se AO
Collections .- --: I RS a AES 467
ppendix 2: New Bnicies of localities
Alp habetic list of localities... .....--. 468
New York localities by counties.-.... 476
a oat a 480
£ record of localities .............-.. 482
i Record of foreign localitiés ......-.. 51
Appendix 3
_ Contact lines of upper Siluric forma-
+ tions on the Brockport and Me-
; dina quadrangles. J. M. CLARKE,
~ R. RUEDEMANN & D. D. LUTHER. 517
_ Paleontologic results of the areal sur-
~ vey of the Olean quadrangle.
ee CLARKE...) 23. 524
_ Potsdam sandstone of the Lake Cham.
plain basin. GILBERT VAN INGEN. 529

. . Graptolite facies of the Beekmantown
t formation in Kensselaer county,
N. Y. RUDOLF RUEDEMANN.... 546

UNIVERSITY OF THE

Mpz1o02m-D1-1500

S HN M. CLARKE State paleontologist |
tae Bulletin 2 };
PALEONTOLOGY 6

w,18

PAGE

Appendix 3 (continued)

-Growth and development of Gonio-
graptus thureaui McCoy. RUDOLF
RUEDEMANN 020 JAWS ols ee

Fossil alga from the Chemung of New
Were, DAWD WHITE... -savess-o 593
A new genus of paleozoic brachiopods,
Eunoa. JOHN M. CLARKE.......- 606
Stratigraphic value of the Portage ~
sandstones. D. D. LUTHER...-- 616
Paleozoic seas and barriers in eastern
North America, E.O. ULRICH &
CHARLES SCHUCHERT J-2- {2.7 ttes 63
Indigene and alien faunas of the New
York Devonic. JOHN M. CLARKE. 664
TGR OA oo igtess is eed gst eee

Plates FACE
1 Memorial tablet on the Emmons
euse, Athany Ni. ¥..- 3.5 cate = 450
Map of portions of s. e. Clinton and
i.e Essex commie. o's ows, 256," 5 99
2 Section along Deep Kill, Rensselaer
ah oi Saha geht = ests ee
Orbiculoidea ma PGW 2 oaly monn we 614
5: A Thamnocladus clarkei White
| 674, 676

5, 6 Eunoa accola Clarke... ......678, 680
7, 8 Orbiculoidea ? magnifica Clarke

682, 684
9 Map showing Paleozoic barriers in

eastern North America. 33

ALBANY?

STATE OF NEW YORK

1902

A9367g

Price 40 cents
o

Watretaw Rew M.A. LLD. me ey Kc

- os epdigenaina M.A. LL.D. ‘M.D. ai
At # by Hewey E. Tunver LL.D.» --'> =>) Se
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jabs Daniet Beacn Ph.D. LL.D. ey, IY ! al
age 8 CarrRoti E. SmitH LL.D. ee, ti ae a

in
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;

ey Bumey T. Sexton LL.D. °° YL. el eee ‘s )
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‘ % 1897 Timotuy L. Wooprurr M.A. Lieutenant Governor, ex -

1899 Joun T. McDonoucu LL.B. LL.D. Secretary of State, ex of ic io
1900 THomas A. Henprick M.A. LL.D. - - — Roches “sig
ae 1901 BenjJAMIN B. OpELL jr LL.D. Governor, ex officio ‘ ry: .
LF 1901 Ropert C. Pruyn M.A. — fe a 2 : Albany ’
7 1902 WILLIAM NotrinGHAM M.A, Ph.D. — a “4 Syracuse ea
‘ One vacancy <¥
yf o
e ‘ SECRETARY

Elected by Regents

1900 JAMES RussELL Parsons jr M.A. LL.D.

DIRECTORS OF DEPARTMENTS

1888 Metvi. Dewey M.A. LL.D. State Library and Home Education
1890 James RusseLtt Parsons yk M.A. LL.D.

Administrative, College and High School Depts 4
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i

_ * —_—s-.

State Paleontologist
es ie

mm Bulletin 52 Rei 1902

| OF THE STATE PALEONTOLOGIST 1901

To the Begone of the University of the State of New York

a have the honor to report herewith on the work of this depart-
ment during the year commencing Oct. 1, 1900.-

Operations in the field 1900-1

Investigation of problems pertaining to the fauna of the Ithaca
5 group of central New York. In my report of last year notice
was taken of the fact that the legislature of that year had pro-
i vided for investigations having special reference to the rela-
_ tions of the Ithaca formation and its fauna to contemporaneous
: organic and inorganic conditions at the east and west of the
central New York area as well as to such conditions as imme-
diately preceded and succeeded them in time. As a preliminary
step to the solution of the problems involved, which were stated
in some fulness in the report referred to, it was essential that
extensive collections be made from the fossiliferous strata
4 throughout the various outcrops of this district. For a large
part of the season of 1900 this work was carried on, specially
in the region from Otsego county westward into the Chenango
valley and into the valley of the Tioughnioga river. The
material sent in as a result of this work, largely acquired by
D. D. Luther, field assistant, was in many respects of high
paleontologic interest, not alone in bringing to our attention
_ organic forms hitherto unknown in our rocks, but specially in
completing series which clearly point to the fact and the course
of development and variation of early species into later. In

-_

(>

2 | eae fossils of this Ithaca tormatee &

representation of this: noteworthy element aa

with the closing of last season’s work, and during th

with the organisms from the rocks beneath, a
the state museum has had only the most. mea

New York faunas. ca
The operations in this part of the state were

of 1901 the investigations, so far as the acquisition of 1
is concerned, have been continued and completed by oe a
the region between the Tioughnioga river and the y
Cayuga lake. This work of collection was carried on by
Hartnagel with the assistance of H. S. Mattimore, _— c
throughout southern Cayuga, western Cortland and ”
counties were carefully exploited.. We have now the x
for the elaboration of various peculiar problems ida om
into view relating to the origin and the destiny of this Ithaca
fauna and also the data for confirming previously expressed
views of its relations to the faunas of contemporaneous age
which adjoin it on the east and west. é st
It may be here of special interest and usefulness to note that
the period of time in which the Ithaca deposits were laid down, :
that is the Portage unit of time, was marked within the limita- 4
tions of the state of New York by the manifestation of at least
three distinet geographic faunal provinces, one in the east, the ~
Oneonta province, where fresh-water conditions prevailed as in
a coastal embayment or lagoon, receiving fresh-water drain-

Eat
me

a.

age from the continental plateau; next west, the province of
the true marine fauna which we know as the Ithaca fauna and
which owes its derivation directly to the fauna which preceded
it in time in this mediterranean sea or Appalachian gulf; and,

ae i =o THE STATE PALEONTOLOGIST 1901 421

- sti fecthor westward, that of the Naples fauna, which is an
5 ‘invasion from the far northwest and occupies all the ground
of | from the meridian of Cayuga lake to the shores of Lake Erie.
_ Furthermore, the region occupied by the invading Naples fauna
ig clearly divisible into two subprovinces, that east of the Gene-
_ see river (Naples subprovince) into which the advance or herald
s species of the fauna penetrated, and the western (Chautauqua)
subprovince, or that beyond the Genesee river, from which the
advance species of the invasion had in notable measure departed
on their journey eastward, but which those following in their
train and pertaining to the same invading body had not passed.
No parallel illustration of the intrusion of so diverse organic
associations or faunas into an area so restricted as that here
concerned between the valley of the Delaware river and the
shores of Lake Erie is recorded so far as our present knowledge
goes.

Study of waterlime strata and their fossil contents. During some
years past study has been made of the character and variation
in the succession of the waterlime series, which in our present
classification of the New York rock series is regarded as per-
taining to the geologic units termed Rondout and Manlius. The
field investigations in this work have been carried on largely by
D. D. Luther, and the results have been important in showing
the degree to which the strata vary in character from one
locality to another, but have been specially profitable in the
hight which they have thrown on the nature of the peculiar
fauna inclosed by these sediments and in the new and interest-
ing contributions to paleontologic facts which they have
brought out. Several of the problems resulting from this series

of field investigations have yet to be carefully studied to be
appreciated in their full significance. Aside from the well
known crustaceans (Eurypterus, Pterygotus, etc.) of these
waterlimes which are produced in such remarkable perfection
and profusion at the cement quarries at Buffalo, and in certain
natural outcrops along the edge of the formation at Union
Springs, Cayuga co., and Jerusalem hill, Herkimer co., the asso-

tice “characters r gies tee “ exar nple as_ Coralline

| Sh LTT:
ae s choharie county and the y of east
“e Ror “The fauna of a ‘specially interes ting outer op of
"8 er appearing on Frontenac island fhicagng 1 lake
calated between the waterlime strata, will, y h
give important aid in the interpretation of the pr

and to which they are otherwise allied, that is to the r
rs bergian strata. Collections were made at and ab put zs
hill, and these operations were not concluded at the
last report. It may be briefly stated that the sum tote
latter work, which was devoted specially to the sew
the crustacean remains at this locality, has afforded 1
interesting and unique material, not only increasing our k
edge of these unusual and peculiar creatures, but also yieldi
important evidence as to their early stages, their a i
deyelopment and habits of life. I note here the fact that from
these collections we have obtained not only the most minute o
these creatures yet recorded, but also the remains of the nite )
heads of Eurypterus not ;)j-inch across, indicating young forms. ina
not above 4 inch in éiitibe length and fragments of a single in.
dividual of the genus Pterygotus which could not have been less —
than 5 to 6 feet in length and thus representing one of the
largest known of all invertebrate fossils, surpassing probably —
in size the similar crustacean, Stylonurus excelsior »
whose parts have been found in the Catskill or late Devonie —
rocks of this state.

‘

Paleontologic and stratigraphic map of Canandaigua lake region.
In pursuance of a widely expressed desire on the part of many |
American geologists that the effort be made to portray on maps
with more exactitude and fulness the paleontologic facts or
actual succession of vital events in the earth’s history, I have

REPORT OF THE STATE PALEONTOLOGIST 1901 425

undertaken to give a representation of such facts in a region

- that has been studied in great detail, perhaps with more care

_, with reference to the succession of its fossil faunas than any

_ other equal area in the state. The early maps of the sedimen-

2 tary rocks of this state, like those prepared in other countries,
combined all available data, organic and physical, for the
delimitation of the formations; but the so called “ geologic
maps ” of today do not attempt the representation of anything
further than the succession of sediments or lithologic units. It
is therefore, not possible that such a map tell the whole truth,
for faunas do not vary pari passu with sediments. These geo-
logic maps representing a succession of-lithologic units display
in a general way, it may be said, the facts which strike the
ordinary observer most forcibly, such as the change in character
of the rock, which may not however harmonize with the registra-
tion of the more essential facts of the earth’s record; they are
properly designated lithologic maps, as they express only varia-
tions in the character of the sedimentation. The true history
of the earth is less the record of the successive changes in the
nature of the materials that enter into the constitution of its
crustal masses and of the physical events which have induced
such changes, than it is a register of succession of the forms
of life which have appeared on the earth in consecutive units
of time. The history of the earth with this vital and organic
element eliminated is the history of a body dead to begin with
and always dead. Let it be invested with the manifestations of
the life force in its manifold variations from the beginning to
the present, and the earth’s history becomes a record of vital
interest.

Experience has further shown in the preparation of geologic
maps in the state of New York, on the scale of the U. S. topo-
graphic base map, that this scale is either too large or our
stratigraphic data are insufficiently refined. The quadrangles,
stratigraphically colored, that we have thus far issued indicate
this fact by displaying for the respective formations represented
very broad bands of color with insufficient differentiation;

- aes

“a | the pao exact that: ete th

study have given us a very detailed knowledge o

i"

ey

have unquestionably served a vse i r
had occasion to employ them. ae
In the region about Canandaigua lake, where 3 rears 0

in sedimentation and the variations in the suecce ge
we have undertaken to color the two -quadrat
as the Canandaigua and Naples sheets, the former 1} ‘ing ing a
north of the latter and giving an area which complet -e
cles that lake and affords a rock succession from ‘the he a
of the Salina gypsum beds upward into the basal. beds o
Chemung, a vertical thickness of about 3000 feet. During t
present season these sheets have been geologically coloe on
the detail of the stratigraphy completed with all practi “al
accuracy; disregarding slight local changes, we have a ound it-
possible to represent variations in the sedimentation i as series
of 26 colors, where, using the ordinary colors hitherto ¢
one for each of the usually recognized formations, nine oe pa
would have sufficed. Corresponding with this detailed strati- 4
graphic map on which it is planned to register every outcrop Be
of the rocks as well as approximately every contact, I have pre-
pared a map on the same base showing the succession and yaria- ‘
tion of faunas, or what may be termed a true paleontologic Pe
map. It is proposed to issue these maps as companion sheets
and to illustrate by means of them the actual relation of major ‘
variations in faunas to variations in sedimentation. In the
field work necessary for the completion of the stratigraphic —
part of this map, D. D. Luther has supplemented the records
made by the paleontologist and himself during the last 20 years.
Areal geology of the Tully quadrangle. Early in the field sea-
son it seemed desirable for the purpose of accurate delineation

AE ee tee ee foe Pe ee cited. ¥ ~ 1S

REPORT OF THD STATP PALEONTOLOGIST 1901 425

PS on the geologic map of the state, and to establish a base mark
or guide for the plotting of the formations immediately above
| and below, to trace the outcrops of the Tully limestone from
Owasco lake eastward into Madison county. Mr Luther was

a engaged for a short time in the work of locating these outcrops
- on the Tully and Cazenovia quadrangles. The Tully topo-
graphic sheet lies directly south of the Syracuse sheet and
covers a very interesting section of the rock series. It has
therefore seemed desirable to complete the areal work on this
sheet, and this will be finished before the close of the present
field season. The field work is in charge of Mr Luther.

Contact lines of formations in the region about Tonawanda and
Oak Orchard creek swamps. The great swamp area lying east
and west along the course of the Tonawanda creek and its
branches and extending to the northeastward along the Oak
Orchard creek and its tributaries, covering a vast acreage in
the territory between Churchville at the east and Buffalo at
the west, a distance of 75 miles, has naturally obscured the
rock geology of a very large area in western New York. The
question as to the direction and position of the actual contact
lines of formations on which this lowland rests came up during
the course of the season in the special consideration of a rela-
tively new member in our succession of faunas lying at the top
of the Niagara escarpment, the so called Guelph fauna of the
Rochester section, to which fuller reference will be presently
made. This depressed region, lying largely between the escarp-
ments of the Lockport dolomites on the north and the Onondaga
limestone on the south, has not been the subject of extended
geologic investigation, and so far as my knowledge extends no
careful traverses of it for the end which has now been in view,
have been made since the early survey of 1836-43. The very
ereat scarcity of outcrops, the depth of the drift mantle, and
the generally unbroken and monotonous aspect of the country
from a geologic point of view, have rendered the attempt to
trace the formational contacts one of some difficulty. The
paleontologist, accompanied by Dr Ruedemann and D. D.

4
yi"
»

&

‘7 the atate hax viaavallingly attor;

>

of vast amounts of soft shale 2 “et gic
leaving as the actual rock bottom of the de or
ment or sill of heavy limestone; thus, by the r emoval oO
Rochester shale which lies on top of the Clinton i ime
deep depressions running east and west along t
these formations were produced, and hence we find th tha at s¢
of the northerly branches of the swamp area, specially those ¢
the Oak Orchard swamp, rest on a bottom of limes tone ag
which this soft shale has been excavated. These areas a
a certain measure cut off from the large area of the
which has been produced by the removal of the soft Salina sl ]
from the limestone or dolomites pertaining to Pe £
formation. Hence the great swamp area generally s spea
lies on a pavement of Lockport dolomite, and by the out ro

-
>" et ee

ping ridges of this dolomite it is more or less distinctly ¢ om 08 a
of these large amounts of soft rock may be teats ascribed oe
erosion by stream action, and we find both in the Tonawanda .
and Oak Orchard creeks—streams whose main courses lie
approximately east and west—a remnant of a force which would
produce and probably has produced depressions of this kind
along the strike of the rocks. While the removal of such large
quantities of soft rock lying between formations of harder and
more resistant texture may be looked on as the occasion for
the existence of these swamps, the cause of their present actual
extent and transgression of geologic barriers is doubtless to be
found largely in more recent damming of the waterways
required by the construction of the Erie canal, obstructing the
natural drainage of the whole territory and rendering the actual

“
Le A ee

run-off insufficient and incomplete. In an appendix to this

me of this work has been to correct in some important par-
_ ticulars these lines as heretofore registered on our geologic
maps. - Because of the scarcity of outcrops, however, the course
q of these contacts may always remain more or less conjectural.
__ Stratigraphic and paleontologic relations of Potsdam sandstone of
4 the Lake Champlain basin to overlying limestones. During some
years past Mr Gilbert van Ingen, special field assistant, has
been concerned with the study of the fauna of the lower lime-
stones of our rock series, specially those of the Beekmantown
and the Chazy horizons as developed in the basin of Lake Cham-
plain. These formations have furnished a large amount of new
evidence as to the constitution of the faunas of the times they
represent. Having acquired special familiarity with the faunas
of these rocks, Mr van Ingen has at my request undertaken
during the last season to study the relations which they bear
to the underlying Potsdam sandstone, and to ascertain in how
far the passage from the latter upward into the former is
gradual and what evidence the fossils afford in regard to the
transition of the earlier fauna to the later. The ultimate pur-
pose of this inquiry is to determine to what degree the fauna
of this ancient Potsdam period bears characters which may
fix its age as Cambric. Historically this well known formation
is the basal member of the “ New York series of formations ”
as enunciated by the four geologists of the early survey. Dr
Ebenezer Emmons, in defending, against the convictions of his
colleagues, the existence of a series of still older fossiliferous
sediments (the Taconic system) did not propose to embrace with
them the Potsdam sandstone, a formation of which he also was
the demonstrator. The Potsdam sandstone is furthermore
clearly a-shallow water or littoral deposit accumulated along
the shelving shores of the most ancient crystalline continent,
and is the oldest deposit of this character of which we have
any knowledge in our rock series. Farther out at sea in the

’ *.
pa

sercean has given a brief ote
problem.

Limestone lenses in the Clinton beds. topes
is made of the fact that one of the icc
investigation by the department, is that relates 0 4
of the peculiar lenses of unstratified semicrysta ine | mes
which have been observed at various outcrops alc omg he
gara cuesta from Lewiston to near Rochester. The se le ati ul
masses of large size, often fully 30 feet in diameter, are
embedded in the well stratified and clearly jointed es
stone, or lie near the upper surface of that limestone a E
overlain by the shales of the Rochester beds. The oceut wt
of these peculiar rock forms, recorded first by Dr- EN ey
Ringueberg of Lockport and subsequently noted by G. Kk &
bert, their nature, origin and faunal composition have’
the subject of study; and it has before been noted that a jetta
of these rock bodies begins near Lewiston on the line ofthe
Rome, Watertown & Ogdensburg railroad, where several are -
exposed, are seen also in beautiful display on the rock face —
along the line of the New York Central railroad just south of — 4
Lewiston, also at Gasport in considerable number, and at Mid- =,
dleport. Dr Ringueberg’s early observations on the faunal con- a

tents of this peculiar rock served to indicate an association in —
i :

some degree foreign to that of the rocks with which it is most

intimately associated but with which it is never blended. The —
fauna is not that of the Clinton rocks of New York nor of the —
Rochester shales; though carrying a considerable representa- — |
tion of these faunas, its most conspicuous species are those —
which have been described as occurring in western faunas —
usually ascribed to the Niagara group. The observations on

, of these lenses has been found at Lockport; on the
of the “gulf” and north of the Niagara road is an
e of several of them lying on the shelf formed by the
limestones. One of these could be located only by pre-
ption, as its site seems to be covered by the embankment
the new electric railroad. Two other lenses are exposed
within a short distance of each other, and these apparently rest
; on the surface of the Clinton ‘limestone. The greatest thick-
; cao of these two bodies was 3 to 4 feet, though this may
have been reduced by long weathering. Compared with the
ee outcrops farther west in the vicinity of Lewiston, these
3 at Lockport did not prove very fossiliferous, the principal fos-
2 sils being Lichenalia and Whitfieldella nitida. The
” lithologic structure of the rock however, a_ subcrystalline,
a _ unstratified mass of hardened, calcareo-magnesian mud, is very

_ characteristic and in harmony with the traits displayed at
a other localities. Heretofore actual exposures of these lenses
5 é have not been recorded at Lockport, Dr Ringueberg’s original
description having cited only loose blocks of this material in
this neighborhood. In the northern part of the city of Lock-
_ port, in the rear of William Stamp’s lot on Jackson street, and
on land owned by Mr Mansfield, several large masses of the
_ Same rock are exposed. These rest on the limestone ledges of
the Clinton, which here form a shelf of some width. This
exposure would seem to indicate not less than two separate
rock bodies.

Between Lockport and Gasport none of these lenses have been
seen, exposures everywhere being unfavorable for their exhibi-

—_

a

“7 1 within the spetg rile, and. thers

A ee ieinis: west of the road. “These all lie in t the uppe
” Clinton limestone, and the majority are | ho n
the stream, the original covering of the limestone h vi
entirely removed, though some still show the covering
of the limestone for a foot or so in thickness, arel -
over the lens, forming a domed surface ofi exposure. “4 As se :
phenomenon is observable in the occurrence on the }
Central railroad at Lewiston, where the arch and 4
formed by the Niagara shale. At Gasport fossils” pore
abundant in the lenses. At Middleport no other evidence o .
lenses is to be found than the single one located by the pe af ae
tologist two years ago and largely removed at that time for th aa |
purpose of obtaining its fossils. This lies on Jeddo creek o1
the land of Mr Ewing and appears to rest on top of the a
Clinton limestone and to be covered by the Rochester oad

ve

Though the shale has been removed from the lens itself, abank

an
of it is not far away, and evidence of it is present about the

edges and on the lower side of the lens. ‘a

There is some evidence of variation in the character of ee. a
fossil contents of these rock bodies, according to geographic
position. Those on the Rome, Watertown & Ogdensburg rail-
road near Lewiston appear to be the most highly fossiliferous

mee eee ee

of all, parts of them being impregnated with masses of sepa-
rated shields of the trilobite Illaenus, which have been —
washed together and piled up like saucers; they are also very ;
rich in cephalopods of unusual species, (Orthoceracones and
Cyrtoceracones), brachiopods, etc. These species are appar-
ently less abundant in the lenses at Middleport and Gasport;
but we are not at present able, from the evidence in hand,
to determine in how far there is a meridional variation in

as over. fea It may be a with comparative security,
a1 t the faunal content was in considerable measure an impor-
ation from the west or southwest. To what degree the sedi-
a= were tidal barriers, and the concentration of the fauna
in this peculiar form due to the dragging action of tidal currents
Por’: “accumulation by other mechanical action, and in how
i far the species represent an actual brief invasion, is yet to be
determined. |
Phenomena of like character to those rock masses are found
in the “Klintar” which constitute striking headlands on the
sea wall of the island of Gothland in the Baltic sea. These are
_-Jenticular masses of dolomites without sedimentation structure,
lying involved in upper Siluric strata of age equivalent to that
of the Clinton and Rochester beds of New York. They have
: - been shown by Wiman! to be the product of reef-building organ-
; isms (corals and bryozoans), though now by wave detrition and
3 by dolomitization but faint trace of such organic structures ap-
pears in the rock itself. The Clinton reefs are so impregnated
} with organisms of form unusual to the contemporaneous de-
posits of the western New York province as to raise the ques-
tion above referred to concerning the influence of tidal currents
jn spreading out on these barriers extralimital organisms from
adjoining provinces.”

+ Ueker silur. Korallenrippe in Gotland. Geol. instit. Upsala. 1897. v.3.
pie, Dp. SL.

* Since the above paragraphs were written, the nature of these peculiar
rock masses of the Clinton beds has been made the subject of a careful
paper prepared by C. J. Sarle (Am. geol. Aug. 1901. p. 282). The author
has registered the occurrence of a considerable number of these rock
bodies and has brought together much evidence confirmatory of their reef
structure.

‘beauty of their preservation, sane
- nodules of white chert found in the pee
a quarry in the southwest part of the a5 tne
_and known as Nellis’s quarry, and also from e xc

ester academy of science, vol. 18. Only an inkling of the —

wie

wa

vs
i

municipal improvements made in the southern s st reets 0
city. Shortly after this discovery a representative seri |
the fossils was submitted to the paleontologist for ex: m
tion, and it was then proposed that a joint deseripti n
interesting new contribution to our New York faunas

be prepared. Subsequently the fauna was carefully | st lie
by its discoverer and brought into comparison with the char: c. : ;
teristic Guelph fauna, which is extensively and © ypiecall ie
developed in the province of Ontario, and the results oe rh
comparison, which did not extend to the details of— ae
identification, were set forth by Prof. Arey on the occasian/. 4 .
referred to, and also published in the proceedings of the Roch- >

presence of such a fauna in the New York rocks had before :
gone on record. As long ago as 1843! Prof. Hall noted the
presence of certain species from what are believed to be the
dolomites of this same horizon; and in that report and in his
subsequent account of these fossils of the Niagara and Salina
rocks in vol. 2 of the Paleontology of New York, they were
ascribed to the beds of the so called “ Onondaga salt group,” the
Salina formation of our present nomenclature. Prof. Hall’s
localities for these fossils were at or near Newark, Wayne co.,
but we have no other than the original record of them. Ex-
posures of this upper narrow horizon along the summit of the

‘Geol, N. Y. 4th dist.

-EPORT OF THD STATE PALEONTOLOGIST 1901 433

al pment are so rare, and the cuesta has been so
trenched either by natural or artificial means, that till
Arey’s discovery, it may be said that we were in almost
ete ignorance of its presence. In and about Rochester
fauna seems to have attained a localized development to a
fusion not observable elsewhere in the state. During the
ast year Prof. Arey has, with great consideration, placed his
collections of those interesting fossils in the hands of the
“pa leontologist for study. We have found that the material
= epresents a fauna of about 50 species, of which 19 appeared
_ (Niagaran) previously in the same locality, 4 are peculiar to the
- congeries itself, and 21 are present in common with the typical
; Guelph fauna of Ontario. It is thus clear that the fauna is not
4 simply a local expression of a late stage of the Lockport dolo-
mite fauna, but represents the true Guelph fauna of Ontario. It
- is possible that the collection we have had in hand does not
3 fully exemplify the fauna, but, as Nellis’s quarry is now aban-

doned, and there appear to be at present no excavations within
the city of Rochester into this formation, we have been at a
loss to add to the material already taken out from this region.
Field investigations have been made with care for the purpose
of tracing this horizon, which, it may be added, is hardly to be
separated from the dolomites beneath by lithologic characters,
to the west and east of the vicinity of Rochester. The most
_ complete section of the dolomites in the immediate vicinity of
the city appears to be that on Allens creek just to the south,
“where shaly layers clearly referable to the basal beds of the

=~ ee

Salina and chocolate colored dolomites which pertain to the
Lockport dolomite series are exposed, but with a covered
interval just where one would expect to find the Guelph horizon.
In transecting the escarpment at various points between
Rochester and Lockport slight traces have been found of the
position—of this stratigraphic horizon, specially at the exca-
vations on the Orchard creek canal feeder south of Shelby,
where the abundant nodules of white chert in the compact dolo-
mite indicate species of similar character to those at Rochester
but in a condition of less satisfactory preservation.

before the stratigraphic etait? of t

‘fully studied by Sir William Logan and Rober
in describing the organisms collected, he referre od he 1
“Onondaga salt group” together with the few 1 |
from what he then believed and what has since prove
same horizon. The Canadian paleontologists, pt :
Whiteaves, have given full accounts of the comp Osi
Guelph fauna, and at the time the collections were de |
those studies, Elora and Hespeler were the most me
the localities; latterly, through a diminished demiudies

rock for construction purposes, less is now accessible at t
localities in favorable condition for exploitation of the f: |
and neither is at present as interesting or productive as. the a
various exposures about the beautiful village of Galt. | as

As shown here, the rock section begins on the east ‘side of
the bank of the Grand river just below the Grand Trunk rail-
road station (Ballantine’s quarry and kiln), where are exposed,
reading from the bottom:

1 A yellow, very sandy dolomite in compact layers carrying 3
Megalomus in immense quantities and numerous gastropods, 10 3
feet;

2 Thinner and grayish slabby dolomites running up to and
above the railroad track, 20 feet;

3 Darker, compact dolomite, 5 feet;

4 Thin, grayish yellow, slabby layers with gastropods, 10
feet.

The entire section from the river bank to the top of the bank
above the limekiln is not less than 55 feet. This locality proved
to be the best in the vicinity for the acquisition of the charac-
teristic fossils of the fauna. The lower layers of yellow dolo-

4

b
m:
ot,

external sate aaa Care pains aa aepen
jamiens a the characteristic exterior eseanee

.

vs ust aac the aie bridge on the east bank
nt, unworked exposure of the upper compact, gray,
aaa which is eee in wie oe Melross’s

Bice a yellow dolomite 15 to 20 feet thick, running
into a heavy bed toward the top. This rock is full of
-Megalomus, but good specimens of other fossils are not common,
and gastropods less frequently seen. This outcrop lies about
_ 2 miles north of Ballantine’s quarry and is probably about 50
- feet higher, completing the section at Galt, which can not be
less than 100 feet thick.
___ All these outcrops are along the strike of the formation, and
Sir William Logan regarded the strata here ag representing the
_ middle part of the group, those at Hespeler on the river Spree
_ being in his judgment below this horizon, while the striking
- natural section at Elora, about the confluence of the Grand and
9 Irvine rivers, where the canyon is not less than 100 feet deep,
_ is considered the summit section of the formation. The series
of fossils obtained from all these Guelph localities will consti-
tute a useful addition to our museum collections.
_ Limestones of the Marcellus stage and origin of their faunas. The
‘Marcellus formation is typically represented by a series of black
bituminous shales, carrying a fauna which has peculiarities so
well marked as to render it readily recognizable. Among these
: shales there occur in different sections interbedded limestones
4 which are specially noteworthy for the diversity of their organic
contents. Thus in eastern sections some 30 feet above the base
_ of the shales lies the series of limestone banks which has been

Phage sated appears at a tigher! orizon in the shales
altogether distinct series of fonifila. "To th his 3 li n estone >
some years ago the geographic name of Stafford li imes 0
find in sections at the very base of the Marcellus se di x n
cially in western New York, still a third impure calez e01
posit which was shown in the section of the Livonia s <9 aft
and recently has been exposed at Stony point south of E sini:
on Lake Erie. This also has a fauna peculiar to itself in n many
respects. Thus we have represented in this period of depos
several quite distinct faunal associations, and they have rai:

the interesting question as to how and whence these faw

have come into our state. The investigation of this propositi
has been in a large measure a summarization of observables a =
made by the paleontologist during the past years, but, in eens:
ing these together for formal expression, much assistance —
has been received from Prin. John D. Wilson of Syracuse, who A
for some years past has been a diligent student of and collector —
from the Agoniatites limestone as exposed in Onondaga mes
and in his work has made some interesting contributions to our
knowledge of the fauna of these layers. Some field operations —
in this connection have also been prosecuted in Schoharie and
Otsego counties with interesting results, as detailed in a paper 7
on this topic, communicated in museum bulletin 49, which is
also accompanied by an account of the section of the Marcellus
limestones as exposed at Lancaster, Erie co., by Miss Elvira
Wood, instructor in paleontology in the Massachusetts institute
of technology, an investigation which the author has executed

ergot ane

with care and exactitude. .
Character of the so called Hudson river beds of the northern

Hudson valley. In continuation of the study of the nature and

composition of the formation which has been known in geologic |

Utica | beds have been ae as far as Mechanieayille. on
the east side the Utica, middle Trenton and Normans kill shale
y \ vere followed only a few miles northward to the long outcrops
on the Deep kill in Rensselaer county. At this point a most
interesting discovery was made in the finding of beds contain-
ing a very unusual graptolite fauna in a fine state of preserva- |
tion ; Such a fauna as was described at an early date by the late
_ Prof. Hall from the so called Quebec shales of Canada. Of this
_ fauna nothing has before been known in the state of New York,
and the presence of these fossils here in such abundance
affords not only important points of correlation of the New
_ York with the Canadian faunas, but again adds in a notable and
d interesting way to the ancient faunas of the state. Though this
fauna is embedded in the “Hudson river slates”, its age as

indicated by the character of its fossils is doubtless to be as-
- eribed to that of the Beekmantown formation, and represents
- in an unbroken succession the faunas of horizons which have
; hitherto in America been known only separately and without
7 any clue to their chronologic sequence. From a biologic point
of view the interest of the discovery is greatly enhanced by the
3 presence of innumerable growth stages representing the entire
_ development phases of many forms, from the embryonic stage
_ to the fully developed colony. This interesting section occurs
near the town of Melrose in northwestern Rensselaer county,
and its graptolites are representatives of the genera Phyllo-
-graptus, Tetragraptus, Loganograptus, Dichograptus, etc.,
which have hitherto been foreign to our faunas. Four different
aggregations of graptolite-bearing shales were found in the
_ thick mass of thin bedded limestones and greenish grits which
_ compose the outcrop; and, as the aggregations or faunules are

| pa Set ae of Diayulogceyeae specis ally D ntti
patulus. ie a ,
2 The next fossil-bearing beds are the ioe in st eci¢
the state of preservation is the most excellent. T
a Tetragraptus and Dichograptus fauna, nearly all he spe
of these genera, which were described by Hall from the ¢ Qt
beds, and several additional ones being present. The f:
these two horizons combined is that reported from ‘ne «
Point Levis zone” of Hall. This has been referred to oti
Calciferous or Beekmantown formation. oe "s -
3 Farther up the creek is another series of graptolite 1 eds is
characterized by Didymograptus bifidus and Phy Sey
lograptus anna, these two species comprising the Pee
jority of all specimens. Neither of them occurs in the first wet bi
horizons, but they are characteristic forms of the Phyllo- — -
graptus anna zone of St Anne river, Quebec. i a
4 Next follows the great mass of the quarry beds consisting a
of heavy banks of greenish grits with thin shaly partings, the s
latter carrying innumerable specimens of Phyllograptu a:
typus, P. anna and P.angustifolius. Besides these
Didymograptus bifidus, D. similis, Thamno-
graptus anna and others. They probably ree the
upper part of the Phyllograptus anna zone. ;
5 About 800 feet farther up the creek are two narrow black
bands intercalated in the dark greenish gray, barren shales,
which carry a very luxuriant assemblage of fossils, having not }
less than 18 species, all of which are new to the New York —

|
faunas. Two of these are brachiopods, viz: Lingula que- |
becensis and a large oboloid representing a new generic ~

aptus. tere D. inutilis,
aptus ensiformis, Cryptograptus
narius, _Retiograptus tentaculatus,
ema, four new species belonging to the rare sub-

: _Desmograptus, piEUSeEY Pens by ere a sin-

i ; es ngly Sistine by the introduction of the diprionid element
ppears to be identical with one mentioned by Prof. Hall as
curring at Point Levis, and which is correlated by Gurley in
his list of the North American graptolites with the upper Beek-
= ‘mantown horizon. Thus the zones which have elsewhere been
held to represent lower, middle and upper Beekmantown hori-
- zons are here exposed in continuous section. It is hoped that
2 more extended study of these beds will furnish the data for an
exact determination and subdivision of the graptolite horizons
‘ throughout the Beekmantown formation, and it is also purposed
4 ‘to present a careful paleontologic study of the graptolites them-
selves. In the appendix to this report Dr Ruedemann analyzes
the section in greater detail and also gives under separate title
an account of the development of one of the graptolite species,
Goniograptus thureaui.

Monroe mastodon. Late last season my attention was called
to the discovery of mastodon bones which had been made some
‘time previously near the village of Monroe, Orange co., on land
‘belonging to Martin Konnight. On visiting the spot, it was
ascertained that the bones found were in the possession of
George Konnight of Monroe and had been taken some years ago,
while drawing muck from a pond bottom which had been ex-
posed by a protracted season of drought. All the bones ob-
tained at that time had been kept together with care by Mr
Konnight. The situation at Monroe was as follows. Just be-
low the-village at the north side of the highway leading to
Turner, lies a pond about 250 feet in diameter containing, at

the times of my visits, water to an average depth of 6 feet. On
<areful study of the topography of the region, it seemed prob-

: Sha ss

‘OTTyYy |

there was no visible Surtaoe inl >t it was
inference that the water was 5 supplied eo: it n nain 5: <
springs in the bottom. K

Among the bones which were in the possession 0
night were the tusks of the upper jaw, which had becor
broken from long exposure but were still in condit at
mounted and which must have been from 8 to 9 feet iné
length, the short tusks of the lower jaw, the occu ites > of
which is of) very great rarity among these fossils, ceveral® ‘ibs,

a scapula, a tibia and other leg bones, some of the bones of t = Fe
feet, etc. all of which except the upper tusks were in a conditi om
of superior preservation. On comparison of their dimensi ns
with those of some of the more complete mastodon ston,
they indicated a skeleton of very great size, almost if not quit é
reaching the size of the Warren mastodon, the largest oy sy
obtained from the surficial deposits of New York. The legis-
lature was asked for an appropriation of $600 to effect the
emptying of the pond and the excavation for the remaining
bones, the fact being recognized that the accumulation of bones. a
from so many parts of the body as were represented by those
in Mr Konnight’s possession, indicated a favorable opportunity
for the acquisition of the remainder. This appropriation having
been granted, the work of emptying the pond was begun i

~<

er ie
Ne

oa t

> ewe iit io a =

June and when all these preliminary operations were concluded
the excavation of the muck in the bottom was begun. The labor
of removing the water and keeping it out of the pond proved —
extremely arduous, as the water was found to enter the pond
by several very large springs, and it was necessary, in order |
to keep the pond basin free of water, to work the gangs at the
pump both night and day. This undertaking eccupied a month

REPORT OF THE STATE PALEONTOLOGIST 1901 441

$ . _or five weeks, and the expense attending it was in excess of the

estimate, so that, when excavation became possible, our means

a did not enable us to carry this to completion. The area of

i about one third of the pond bottom was carefully dug over, and

Pee a Vey eae ee 22 ese. bt." 7 Pe ce er ne
‘ ue 2 Se en a ee

additional evidences of the mastodon skeleton were found; but,

as we had reached the limit of our appropriation and were in

danger of passing beyond it and incurring an expense which
could not well be borne, and as I was unable to obtain additional
assistance from any private source, it became necessary for us
to end the work with the excavations incomplete. Hunting
‘mastodon skeletons carries with it a large element of uncer-

_ tainty, as such skeletons are very rarely complete. The fluidity

of the soil in which they have become mired disjoints and scat-
ters the bones, with the result that the finding of one part or
a considerable portion of a skeleton does not guarantee the
presence of all the bones. The parts we have obtained have
features of considerable interest, specially the lower incisors
to which reference has been made, and the possibility of re-
claiming the remainder of the bones is still about as good as
it was at the beginning of the enterprise.

Cooperative work with the U. S. geological survey on the Sala-
manca quadrangle. In the season of 1900 the work which had
been undertaken on the areal geology of the Olean topographic
sheet was brought to completion, and the results carefully
worked out both here and by the representative of the U.S. geo-
logical survey, Prof. L. C. Glenn. This work and report thereon
will be published during the coming year. With the opening of
the present season the work was continued to the adjoining
quadrangle on the west (Salamanca), in which Prof. Glenn was
associated with Myron L. Fuller of the U.S. geological survey.
Charles Butts, who had during the previous season been the
representative of this department in that work and who had
prosecuted the stratigraphic and paleontologic determinations
in the office during the winter, had in the meantime received
an appointment as assistant geologist on the U. S. geological
survey, but by the concession of M. R. Campbell, geologist in

E there remains uae ‘izatior
_ and the detailed SSyceeaitaieen of the st tratigray
- graphic sheets. This will be the work aurtag ee

. ons “euaty <n eines | i. a *
a 7 P ©
“The it ae 5

a ve : .
: ye '
; ce

sat e
a ~~

of Prof. L. C. Glenn, and the completed map will b
eated to this department for publication, together 1
planatory statement of the detailed stratigraphic 0
Further reference is made under the head of office work Ee 7
of the paleontologic and stratigraphic results obtained f t
work on the Olean sheet. ae m a

Personnel of the field staff

In the field operations of the department during the last 8 a

son the following men, outside the permanent staff of the 4 rae
partment, have been engaged: Prof. Charles Butts and } a
Myron L. Fuller of the U. 8S. geological survey, on “the
work in Cattaraugus county; Prof. A. W. Grabau of Columbia —

university with H. W. Shimer of Columbia university, R. Kr
Morgan of Buffalo, Charles Ewing of Middleport and T. W. Pier-
son of Lockport on the investigation of the Clinton lenses in

Niagara county; Gilbert van Ingen in the study of the lower —
Siluric of the Champlain basin; C. A. Hartnagel of Hornellsville
on the Ithaca group problems in Tompkins and adjoining
counties.

-
.

© ee
‘a
,
Fs sa
or
i
"3
4,

Office work

Publications. The reports which were left unfinished at the
time of the death of the late state geologist and paleontologist,
Prof. James Hall, have now been brought to a conclusion and
are all printed and issued. In regard to the memoir on the
Generic structure of the Paleozoic corals which Prof. Hall had
planned, I am able to report additional progress in spite of

—— ee eS es oe - —

REPORT OF THD STATE PALEONTOLOGIST 1901 443

: oo the incertitude involving many of the specimens on which the
investigations have been based, partly with reference to their
‘if cactual geologic position and partly relating to their geographic
locality. The material with which it was expected that the
a investigations would be continued belonged largely to the col-
lection of Prof. Hall, and only a small part of this material has

been since his death available for these studies. Notwithstand-
ing these and other difficulties pertaining to its execution, I be-
lieve it practicable to present this subject in a form useful to
students.

During the last year the following publications have issued
from the department:
_ The annual reports for the years 1899 and 1900.

Museum bulletin 39, containing a number of papers relating
to paleontologic and stratigraphic problems, as follows:

A remarkable occurrence of Orthoceras in the Oneonta beds
of the Chenango valley, N. Y.;

Paropsonema cryptophya, a peculiar echinoderm
from the Intumescens-zone (Portage beds) of western New York;

Dictyonine hexactinellid sponges from the Upper Devonic of
New York, and

The water biscuit of Squaw island, Canandaigua lake, N. Y.,
by John M. Clarke;

Preliminary descriptions of new genera of Paleozoic rugose
corals, by George B. Simpson;

Siluric fungi from western New York, by Frederick B. Loomis.

Museum bulletin 42, entitled the Hudson river beds near
Albany and their taxonomic equivalents, by R. Ruedemann.

Museum memoir 3, entitled the Oriskany fauna of Becraft
mountain, Columbia co. N. Y., by John M. Clarke.

Museum bulletin 45, Guide to the geology and paleontology
of Niagara falls, by A. W. Grabau.

New agelacrinites, a , Py:
Amnigenia as an indicator of fresh-water ¢ a agi
the Devonic of New York, Ireland and the Rhine’ ‘la ad, by
M. Clarke; am pee
Marcellus limestones of Lancaster, Erie co., N. ¥., by
Wood. wv =
Bulletin (as yet without number) being a catalogue 4
types of Paleozoic fossils belopemg to the New vork'@
museum. re

a
With reference to the last named cibtication i enter - is
some further detail. be Le. a
Catalogue of type specimens. For nearly three years, as OPP 0
tunity has afforded, we have been carefully compiling a ca va
logue of the type specimens of the Paleozoic fossils of 1 he
museum collections. Though many of these important obje
had been brought together by themselves, a large number were a
found to be scattered, sometimes without distinguishing mark,
through the collections both in the State hall and in Geological
hall. It has consequently been an onerous task to identify —
these and bring them together. This work is now virtually —
done, and we have in press at the present writing the completed
catalogue of all of this valuable material. It is the purpose to —
present this catalogue in a broad. biologic arrangement and to
supplement this with tables showing the geologic distribution
of the organisms through the rock series. While probably
every year will subject the list to supplementary additions, —
as the work progresses or as more careful examination of our
extensive collections reveals additional type specimens, at the
present time the following is a statement of our possessions of

this kind.

ais

= Vermes:
_ Crustacea . 6438
. a Pisces — | ane ses SATS

ae city; pie from this fact the impression has in some
: _ measure gone abroad that the greater number of types of the
te Paleontology of New York are not in Albany but in the museum
at New York. It is therefore perhaps appropriate that atten-
tion be here directed to the following statement with reference
_ to what may be termed types of the New York paleontology in
"the possession of these two museums, lest misapprehension
"continue in regard to the location of such specimens. The cura-
tors of the collections of Paleozoic fossils in the American
_ Museum of natural history have recently published a detailed
catalogue of their type specimens from which we draw the
| ‘ following:

3 Total number of type specimens, Cambric to Devonic inclusive,
4067. Of these the types figured in official New York state
publications are 3626; types from the Paleozoic rocks of New
_ York state figured in official state publications, 2696.

—

15 \ tae alia

+ year Mr ©. A. Hartnagel v was engaged omp
- eard catalogue of the fossil faunas of pat our | pa
‘Such lists have never been prepared, and a catalos at
to me imperative to enable us to note in how pie
lections retain the recorded representation of t nes se faun

lists. The work is however not merely one of compi pilation.
requires for its perfection much careful review, and the e lim!
tion of the synonymous names, and really for its best u
ness, a grouping which shall be a better expression 0
relations of the faunas than the mere bringing together a a
‘species under the general names of the formations. a li ists
are very large, running up into the thousands of species, baie
is believed that it will serve a useful purpose to put this event
ually in published form, as has been done for the ancient a a
of other countries. ae ae

Determination of Rochester shale fossils from western New York.
Mr Hartnagel was engaged for part of the year on the deter-
mination of the fossils contained in a large amount of material
‘brought in from the Rochester shale of Middleport and other
localities in western New York. As the representation of the 9
fossils of this formation in the state museum has heretofore
been somewhat meager, though containing many fine examples,
this work has served to extend our knowledge of the fauna and
has added a number of hitherto unrepresented species to our
collections.

Study of fossils of the Ithaca formation. In connection with the
problems relating to the Ithaca fauna, to which fuller reference
has already been made, Mr Charles Butts was engaged for some
time on the identification of the material collected during the
season of 1900. Mr Butts’s familiarity with the species of the

7

ae between a Hamilton shales beneath and the
E: Genesee shales above. This pyrite is usually very compact
and hard, and in many places among the twigs, balls and pellets.
lof evidently concretionary nature are entangled considerable
_ numbers of diminutive fossils. At the meeting of the American
association for the advancement of science at Columbus in 1899,
q the writer called attention to this peculiar occurrence in the
_ hope of eliciting some expression as to the probable origin of
q such a continuous deposit of this peculiar nature extending un-
_ broken for almost 100 miles. Considering that the deposit pre-
4 ceded a period of evidently shallow, inclosed coastal areas or
3 embayments, where organic decomposition proceeded in such @
_ manner as to impregnate the muds with bituminous matter
} (represented in the black shales of the Genesee), it seemed
natural to conclude that the environment which conditioned the
formation of this iron sulfid was also due to excessive organic
_ decomposition with generous liberation of iron oxids.

As long ago as 1885 the writer described a considerable num-
ber of organisms from this pyrite layer, recognizing the fact
that they presented similarities to species of the preceding or
Hamilton fauna, but their diminutive form seemed to render
actual identification of them with previously known species in-
secure, and hence for the most part they were described as new

way tech their vaecalielee that is to say, with @
_ tions all have a diminutive size which may express a
of function or an arrest of development. Some time ago I
Dr F. B. Loomis of the biologic department of Amherst col
to undertake the investigation of this problem. He has stu
the matter with much care with material from varloaes ter
of the pyrite layer, has been enabled to free the org r
identify them, and by a series of experiments has dragn «
interesting conclusions as to the causes which have mc ms | ee
them and the conditions which prevailed over the sea botto: a
during the period of their life. Dr Loomis’s results. will | 4
given in a future report. aa

Contributions to the geologic map of the state. In the compila- ag
tion of a geologic map of the state by the state geologist, Nei
have been pleased to place at his disposal all the data in the
possession of this department which could in any way serve to |
render more accurate the delineation of the formational contact
lines among the sedimentary rocks. These facts were those —
accumulated for this purpose by the late Prof. Hall and partly
by myself under his supervision or independently. For the sake
of the accuracy of this official map, I have also undertaken the
determination by active field observations of some doubtful
points, all in the hope that this map may, so far as the sedi-
mentary rocks are concerned, express our best and most ac-
curate knowledge of their distribution and classification.

Index to state publications on paleontology. The University has
undertaken the preparation of an index or series of indexes to

ie
=
wel oe,
‘Sy

.

ee Se eee eee eae

tee ee Oi Beem

=< ze | |
ntifie papers issued under its supervision. To make this

York, I have undertaken to compile detailed references to
extensive literature of this subject, including references
descriptions of genera and species. To meet fullythe purpose
of such a compilation, it has seemed highly desirable that in this
‘regard the list shall be exhaustive. The undertaking ig one re-
quiring considerable time, and it has been thus far carried for-
ward in the intervals of more pressing work by Jacob Van
- Deloo, the clerk to the department.
Contraction of office quarters. Mar. 18, 1901, a bill was intro-
duced in the assembly repealing ch. 355 of the laws of 1883, giv-
3 ing to the board of regents the supervision and control of such
_ Tooms in the State hall as were then or were to be occupied by
_ the state museum. Apparent necessity for this legislation arose
3 from the demand for room on the part of the state controller,
the work of whose department had in certain directions become
greatly enlarged by recent legislation. Before this bill passed
the legislature, as it eventually did, provision was made in the
supply bill to move the offices of the paleontologist and his
staff to the second floor of the Geological hall. The items for
this expense did not however meet the approval of the gover-
nor. Though we were thus left undisturbed, I desire to record
here the fact that, at the time this proposition to remove our
quarters was made, we occupied offices in the State hall with
a floor space of 6822 square feet, divided among six rooms on
the third floor and two rooms in the basement. Of the third
floor rooms three of the largest were unsuited for any other
purpose than storage on account of insufficient light. These
With al] the rest were filled with stacks of drawers containing
the synoptic and special collections of the department. It was
calculated at the time that the actual weight of the paleon-
tologic specimens in this building, together with all movable fur-
nishings and appurtenances of the department, was more than
250 tons. The failure of the appropriation referred to did not
lessen the controller’s need for more room; and, as the legis-

eS eee Fe

=

: es Ss pe og eee ae a = rs
F THE STATE PALPONTOLOGIST 1901 149

plete as possible in its references to the paleontology of

Se

eh

“es

DELS

ht. canals: i tai
’ FY) Re’ nae a se He < As; ary
: evi _ 4

’ “the embarrassient to 00 wo

space to render our , speciall;
accruing from field work in sraaol .
study. It has been a source of pede, increasin
to adjust ourselves to these restricted and hampering di
However, in response to the controller’s wishes, , | Wi ot ‘

- sacrificed 2000 square feet of floor space, PS aa nt

three well lighted rooms, and, with all our effects in > t 1e 0
tracted space remaining, are endeavoring to carry forw ar Oul
work and to find place for our constantly growing | co) a

The accessions accruing annually from necessary pris
tions are large, as these reports indicate; and the proposi
return to Geological hall, after having left it 20 years. aget
cause the building was then regarded as overcrowded, involves
a serious step backward. It is needless for me, under thes
oppressive surroundings, to renew a plea for appropriate q
ters. The condition itself is an acute appeal therefor. Such
quarters will come only with the construction of a modern and
suitably equipped building for the museum, and this condition —
seems to be fully appreciated by all the friends of the institae
tion.

Exhibit of the department at the Pan-American exposition. ‘The —
department was called on to prepare an exhibit for the exposi-—
tion at Buffalo. In response to this request an effort was wea
to bring together:

1 A series of the publications of the state relating to paleon-
tology and stratigraphy.

2 The geologic maps issued by the department on the a 7

Sie
:

ad
~ ww
-
~,
=

graphic quadrangles.
8 A series of the original drawings and plates of lithographs:
used in these publications. leis

e 0, e ee fe this occasion an :
1id = the st qd paleontology of the Niagara

the aa known cement quarries at Buffalo; and it is safe to
that no such collection of these remarkable and interesting
“objects: was ever before brought together in one place. Great

eredit and much gratitude are due to the generosity of the
| - Buffalo society in allowing their material from these rocks to
be exhibited with that of the state museum in the completion

_ of this series. | cha

_ As a second exhibit of this kind, an extensive collection was
3 prepared, to represent the fossil glass sponges which were the
subject of a recently published state museum memoir. Here
9% again we are placed under many obligations by the great
eonsideration of E. B. Hall of Wellsville, the owner of a large
_ number of characteristic and beautiful specimens of these fos-
sils, which we supplemented in a measure with material from
the state museum.

In the preparation of the guide to the geology and paleon-
tology of Niagara falls and vicinity, we again had the cooper-
ation of the Buffalo society of natural sciences. This
work was placed in charge of Prof. A. W. Grabau,
who made a special resurvey of the region and some
4 ‘special collections of fossils. The work was designed to
treat of the origin of Niagara falls, its history and development,
and incidentally the development of the topography of the ad-
‘joining region; a considerable part of the work was devoted to
the stratigraphy and the character of the fossils, with abundant
illustrations of all the species known to occur in the exposures
along the gorge. Asa whole the guide seemed well adapted

of the ‘Anienicaar ausoael he advancement |
its Denver meeting, peat, 1901, au thori izing th e pl
bronze tablet on the house Te tently was” tl
Dr Ebenezer Emmons, state geologist of New York k in
of the second geological district, 1836-42, to commemor
that the association looks on this house as the p ;
inception. The events leading up to this action are |
in the following document, which is the report and re “01
tion made by the committee of the American associatic
the advancement of science, and adopted by that body. re

~s

Report OF COMMITTER OF AMERICAN ASSOCIATION FOR 1
ADVANCEMENT OF SCIEPNCE ON THE EMMONS HOUSE MEMORIAL |

The American association for the advancement of. OES
organized in 1847. It was the organic descendant and onliire ed
outgrowth from the Association of American geologists and —
naturalists. The latter body was created in 1842 by the —
incorporation of the naturalists within the Association of
American geologists. The Association of American geologists —
is therefore to be looked upon as the legitimate organic ancestor
of the American association for the advancement of science. =

The cireumstances which led up to the organization of the —
Association of American geologists are as follows: |

During the prosecution of the geological survey of the state
of New York the need of the geologists for consultation and ~
interchange of view with others engaged in official geologic
work led to the suggestion of an organization of a body of
American geologists.

It appears that Lieut. W. W. Mather, one of the New York
geologists, suggested the subject of such a meeting to the-
board of geologists in November 1838. He wrote:

“ Would it not be well to suggest the propriety of a meeting
of the geologists and other scientific men of our country at
some central point next fall, say in New York or Philadelphia?
There are many questions in our geology that will receive new
light from friendly discussion and the combined observation of

--REPORT OF THE STATE PALEONTOLOGIST 1901 453

‘ious individuals who have noted them in different parts of
r country. Such a meeting has been suggested by Prof.
heock, and to me it seems desirable. It would undoubtedly
an advantage not only to science but to the several surveys
it are now in progress and that may in future be organized.
t would tend to make known our scientific men to each other
ersonally, give them more confidence in each other and cause
them to concentrate their observations on those questions that
are of interest either in a scientific or economical point of view.
More questions may be satisfactorily settled in a day by oral
_ discussion in such a body than in a year by writing and publica-
tion.” (Letter from W. W. Mather to the geological board of
§ New. York, dated Nov. 9, 1838, and addressed to Prof. Emmons)
It appears herein that the suggestion of this meeting was
originally made by Pres. Edward Hitchcock of Massachusetts,
_ who was the first to receive the appointment as geologist of the
first district of New York from Gov. Marcy. Pres. Hitchcock
_ has said in regard to the suggestion made by Lieut. Mather:
_ “As to the credit he has here given me of having previously
_ suggested the subject, I can only say that I had been in the
habit for several years of making this meeting of scientific men
a sort of hobby in my correspondence with such.”!
Lieut. Mather’s letter to the board of geologists was taken
up for consideration at a meeting held Nov. 20, 1838, at the
house of Dr Ebenezer Emmons, corner of High st. and Hudson
ay., Albany.”

The action taken by the geologists was one of unanimous
approval of the proposition, and Lardner Vanuxem of the third
district was commissioned to open communication with other
geologists, specially with Pres. Hitchcock, with reference to
carrying this project into effect. The undertaking was not
immediately successful, and at a meeting held in the autumn of
1839 the purpose of the geological board was reiterated. This
meeting was also held at Dr Emmons’s house, the four geolo-
gists and the paleontologist being present, and also Ebenezer
Emmons jr, who still survives. As aresult of the second under-
taking on the part of the New York geologists, a meeting was
called in Philadelphia for April 1840, where and when the
organization of the Association of American geologists was
effected. The following year the association again met in Phila-
delphia, when the membership of the body was largely increased,
*Address of Pres. Edward Hitchcock at the inauguration of Geological
hall at Albany, Aug. 27, 1856. N. Y. state cabinet of natural history. 10th
ma rept. 1857. p. 23.

*See documents hereto appended, being A, a statement dictated by Prof.
James Hall, Aug. 24, 1896, and B, a statement dictated by Ebenezer
Emmons jr February 1900.

1 EE ae ey ee

454 NEW YORK STATE MUSEUM

and in 1842 the place of meeting was Boston, and the
already rehearsed, both the name and scope of the association
were, at the solicitation of the naturalists, enlarged. Pres-

Hitchcock, addressing the New York public interested in the ~
outcome of the work of their geologists, makes the following —
statement in the address already quoted: am

“It may be thought that the New York geologists in their 1
invitation and the members of that first Philadelphia meeting —
had no thought of extending their association beyond geolo- ’
gists; but Prof. Mather’s language just quoted speaks of fa
meeting of the geologists and other scientific men of our
country’, thus showing what were his aspirations, and they
were shared by all of us who had anything to do with that first
meeting. But we knew that only a short time previous the
American academy of arts and sciences at Boston had directed
a request to the American philosophical society as the oldest
of the kind in the country, that it would invite the scientific
men of the land to such a meeting as the one we are now enjoy-
ing; but the distinguished men of that society declined through
fear that the effort would prove a failure. Surely then it did
not become us to announce any such intentions or expectations;
yet we did talk of them and could not but hope that what might
fail if attempted on a large scale at first might be accomplished
step by step. Had not the New York geologists issued that modest
invitation and confined it at first to the state surveyors, probably
even yet we might have been without an Association for the advance-
ment of science.’’}

The committee appointed by this association to coneien the
matter of placing a memorial tablet on the Emmons house in
Albany N. Y. begs to submit the foregoing as evidence of the
prenatal history of the American association and to recommend
that this house, the home of the late Ebenezer Emmons, a man
of eminence in his profession, of untiring diligence and endur-
ing patience, be permanently marked by a tablet setting forth
the interest of that spot to the history of the association. It
is suggested that such tablet bear the following inscription:

IN THIS HOUSB, THE HOME OF
. DR EBENEZER EMMONS,
THE FIRST FORMAL PFFORTS WERE MADB, IN
1838 AND 1839, TOWARD THE ORGANIZATION OF THB
ASSOCIATION OF AMERICAN GEOLOGISTS,
THE PARDPNT BODY OF THE
AMERICAN ASSOCIATION FOR THE ADVANCEMENT OF SCIPNCBE,
BY WHOSE AUTHORITY THIS TABLET IS BPRDPCTED.
1901

— — — ————

*Address of Pres. Edward Hitchcock, as cited.

a ‘ Want et cost of ks tablet

n on ve ey of the association but

=f Joun M. aye Chairman
art CO; FA. Peer o :

9 McK. Catreitni

oe J. McGne —

aa “ ies 24, 1896.
es The organization of a body of American geologists was pro-
posed: by the four geologists at Dr Emmons’s house at the
; corner of Hudson ay. and High st. It was during the fall of
- 1838. Vanuxem was asked to see or communicate with the
_ Rogerses concerning it, but nothing came of it that year: The
- next year we eee ed our purpose, as the intention was to
get some means of comparing our results with those of other
q geologists in other states, especially in Pennsylvania. This
- meeting was held at Dr Emmrens’s house, the four geologists
_ being present and perhaps also Conrad. Ebenezer Emmons jr
was also there. We then decided to communicate again
with the Rogerses and others for the end already suggested
and to organize a society of geologists for this especial purpose.
_ We wanted to compare our results with those of others and
make up our nomenclature, and we had to do it soon as we were
required to publish. As a result of this unanimously expressed
_ purpose, a meeting was called for April 1840 in Philadelphia.
I was present then but not at the second Philadelphia meet-
ing in 1841, as that year I was off in May and June with D. D.
Owen on a flatboat sailing down the Ohio, sleeping on a box
and collecting fossils all along from Louisville to New Har-
mony. As far as Rogers was concerned the meeting came to
naught. He was not ready with his results and gave them
only at the third meeting at Boston in 1842. It was here that
the naturalists proposed to join us, and we agreed thereto,
but the Boston meeting was called as the meeting of the Asso-
ciation of American geologists, and in the course of that meet-
ing the name was changed to that of Association of American
geologists and naturalists.

B. Statement dictated to John M. Clarke by Ebenezer

Emmons jr, February 1900.

I was present at the meeting of the four geologists at my
father’s house, in 1838. I was then about 16 years old, and
had assisted my father in his field work and making drawings

we

a ee eee eee ae

pty of Heasah p av. and ngs bs
Sl in some measure ie serie et
state geologists of the geolog ri

Peroounel of foo stall

‘The staff of the office has remained as pee
addition to permanent position of D. D. Luther”
interruptedly employed in the department since Ls } as

Rudolf Ruedemann, assistant paleontologist

D. D. Luther, field assistant

George B. Simpson, draftsman

Philip Ast, lithographer

Jacob Van Deloo, clerk i

H. 8S. Mattimore, preparator and page

Martin Sheehy, machinist Ac :

Prof. Charles Butts and C. A. Hartnagel have been ¢ em ple
for parts of the year on special work. e

It is with sincere regret that I have to record the dee
Oct. 15, 1901, of George B. Simpson, draftsman, after an i |
which kept him but a few days from his duties. The loss of Mr |
Simpson’s important services is a serious deprivation to the work
of the department.

Locality record of museum specimens

In continuation of the record of fossil-producing localities,
parts of which have been communicated in my last two reports, —
I herewith submit a list of the additional localities entered —
during the course of the last year’s work.

21 Oct. 1901 Respectfully submitted

JoHN M. CLARKE
State paleontologist

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REPORT OF THE STATE PALEONTOLOGIST 1901 457

Be ||
George Bancroft Simpson

1844-1901 |
George B. Simpson was born at Boston Mass. Nov. 1, 1844.
His father was a mechanical genius and inventor and, though
not fortunate in the affairs of this world, was a high-minded
man, of upright life and a pillar of the methodist church.
His mother was a woman of strong character, genial and
lovable disposition. She was the sister of the late Prof.
James Hall. Mr Simpson in his young manhood appren-
ticed himself to a printer, but soon after the breaking
out of the civil war, he enlisted for the service, enrolling
with Company F, 68th Illinois volunteers, on the 5th of June,
1862. He served with his company for the full term of his en-
listment, turning in his bounty and pay to the support of the

_home, which had then been moved to Waterbury Ct. After

his first discharge he came to Albany and was for a brief time
employed by Prof. Hall as a collector of fossils, but he soon re-
enlisted, this time volunteering with the 106th New York
infantry, and served therewith till the end of the war. He then
entered Yale college, having an ambition for the law, but finan-
cial misfortunes fell on the home and were closely followed by
the death of the father, so that the cherished hope had to be
abandoned, and the young man left college to seek his own and
his mother’s fortune and to maintain the homestead at Water-
bury. He turned to his uncle in Albany, and then, 1868, at the
Suggestion of Prof. Hall and under the tutelage of the artists
who were employed on the paleontologic work of the state,
Mr F. H. Swinton and Prof. R. P. Whitfield, he undertook the
drawing of fossils for these publications. Here he remained till
his death, except for an absence of two years in Pennsylvania,
when he was engaged on similar work for the second geological
survey of that state.

Mr Simpson’s nature was sensitive and retiring, and he was
more inclined to shun than seek companionship, so that very
few saw the true spirit of the man or realized the motive of his
life. Such men, failing-to enforce a recognition of their real

et Healy the beat ese
his mother. In her oe cent $
fc apatatomabig, for laudation and path anat ‘on or hh her =f
home at Waterbury he provided to the end of her lif
this excellent woman and his good father he seemed to
inherited many fine traits of character, a strict integ arity
conscientious punctiliousness and perhaps also his. deli
nature and all her works. In his work of preparing scleé
‘drawings of paleontologic objects he succeeded for ac r
expression and of detail far beyond his own expec te
-ing,a power that few have equaled. The thousands of ¢ :
ings which he made for the Paleontology of New York conte ed “a
in a most important way to the value and prestige of that work, 5
Less can not be said than that he was the vehicle for the proper —
expression of our paleontologic data; and many a working ©
paleontologist has allowed himself to express the feeling that *
a publication, specially of a descriptive character, is less serv-
iceable without the illustrations than the illustrations without
the description. On looking at some of his most skilful and
elaborate drawings of crustaceans and plants from the Coal |
Measures, Prof. Lesley, the former state geologist of Pennsyl-
vania, expressed his amazement that such execution was within
human power; and yet but few saw the results of Mr Simpson’s
handiwork save after they had passed through the printing
press and were shorn of their finer beauties. Mr Simpson was
draftsman less of choice than of necessity. Had his way been
-elear before him and the preliminary training attainable, his
deep seated, never lessening love of nature would have carried
him to successful accomplishment in some branch of natural *
history. The flowers were his constant companions; he seemed
to crave their unspoken sympathy, and knew and loved their
haunts. When he painted them, it was with a preraphaelite
touch that was startling in the exactitude of detail.

ee.

and in much more gerious and substantial manner in his pub-

eye ee ee er
as 2 ns wee

eS “es ~ .*

lished demonstrations of the anatomy of the fresh-water clam

(Anatomy and physiology of Anodonta fluviatilis, 35th rep’t N. Y.
gtate mus. 1884. p. 169-91, pl. 1-11) and in a beautiful and still

more elaborate memoir on the anatomy of the snails (Anatomy and
physiology of Polygyra albolabris and Limax maximus and embry-

ology of Limax maximus,N. Y. state mus. bul. 40) which he did not

live to see in published form, but of which almost his !ast con-
scious act was to read the proof sheets. One naturally turns first
to the illustrations of these papers; and it is worthy of remark
that the drawings of this memoir on the snails are the most
highly finished that ever came from its author’s hands. They
were marvels of handiwork and have elicited unstinted praise
from expert students of the Mollusca. They have proved, how-
ever, beyond the capacity of the printers to reproduce and have
hence lost much of their beauty. These works demonstrated
Mr Simpson’s natural taste for scientific investigation.

In the execution of the various volumes on the Paleontology
of New York, Prof. Hall planned one on the Bryozoa, a group of
lowly molluscoid organisms which abounded in profusion in the
old faunas of New York. The drawing of these organisms re-
quired great skill and much study, and it naturally followed
that the draftsman acquired a close familiarity with this multi-
tude of specific forms, their variations and mutual relations.
He became in fact more familiar with them than any one else
could become without long and laborious study; and as a con-
sequence Mr Simpson was the virtual author of vol. 6 of the
Paleontology of New York, which was almost exclusively con-
cerned with these organisms, and not only of this but of all the
descriptive matter pertaining to these fossils published during
the decade from 1880 to 1890. One outcome of this work was
the Handbook of North American Paleozoic Bryozoa, published by
Mr Simpson, the usefulness of which to many students can not
be gainsaid. All these publications on the Bryozoa were sub-
stantial contributions to the paleontology of the ancient rocks,

—

acters. Mr Siaplongengiclan escriptive m
to the corals published from 1880 to 1890. eas
the death of Prof. Hall material was being gathered Jn 1d
for a more comprehensive. memoir on the genera be sp
the extinct corals; and on the drawings and desorlly ‘iy ve pa
this work Mr Simpson labored faithfully to within a few m
of his death. Thus in this field too we shall find ourse: va
much to his fine powers of observation. ae
Mr Simpson married in 1891 Miss Abigail L. Soule, w
vives him. ~ ee
dX
ee aL |: an

- i

“3 .- ie s

ye ot

le “e D., U. S. national museum
Specimens of B eltina danai
See Wale. Belt series (pre- -Cambric) Glen-
- 2 - wood and Neihart Mont. 25
Derby, 0. A., Sao Paulo, Brazil
3 _ Notothyris ? smithi Derby.
ade Middle Devonic, Matto Grosso,
Brazil. | 3
Bennett, L. J., Buffalo
: Pterygotus and Eurypterus. Water-
lime, Buffalo. , 3
Wilson, J. D., Syracuse
Thoracoceras wilsoni Clarke.
; Agoniatites limestone, Manlius.
- P ayarty, C. K., Bellevue O.
Fossils from Onondaga limestone.
Stafford. 2
Loomis, F. B., Amherst Mass.
Fossils from Clinton limestone:
Peronosporites ramosus
Loomis
P. globosus Loomis
P. minutus Loomis

Te

(4 types)

}
4 (4 types)
|
J

Do: 1us

Pleurotomaria es Reva
ginata var. Hamilton beds,
Port Jervis.

“The paleontologist
A eollection of fossils from various

New York localities of the Helder-
berg and Onondaga limestones, the
Marcellus shales, Hamilton, Gene-
see, Naples, Oneonta and Chemung
beds; together with specimens of
minerals (200) and Indian relics :
(450). 5 296

This collection includes the following
type specimens:
Crustacea (Hamilton)
Goniatites (Genesee and Naples)
Lamellibranchs (Genesee and Naples)
Miscellaneous (Naples)
Miscellaneous (Genesee)

‘Hall, E. B., Wellsville
Chemung fossils from Broome co.
Davis, E. E., Norwich
Fossils from the Ithaca formation
near Norwich and Coventry.
Psaronius. Large specimen from One-
onta sandstone, Oxford.
Chadwick, G. H., Catskill
Paropsonema cryptophya,
from Naples beds, Hicks’s gully,
Canandaigua lake.

aad

REPORT OF THE STATE PALBONTOLOGIST 1901 463.

Fossils from Oneonta shales near
Lawrence station, Greene co. 3

- ‘Wood, Elvira, Waltham Mass.

Fossils from the Stafford limestone,
Lancaster, Erie co.
Carnia recta Wood
Ambocoelia nana ?Grabau

Gordon, Robert H., Cumberland Md.

Goniatites from the Marcellus shales
at Cumberland and Corrigansville
Md.

Clark, W. B.,

Fossils from the Jennings formation,
western Maryland.

Total by donation

Purchases

The S. W. Ford collection of Cambric fossils:

Palaeophycus incipiens Bill,
Troy

Archaeocyathus rarus Ford,
Troy

A. rensselaericus Ford, Troy

Ethmophyllum ? (cast), Troy

Lingulella caelata Hall, Troy

Obolella crassa Hall, Troy

Obolella crassa Hall, Lansing-
burg

O. gemma Bill., Troy

O. nhitida Ford, Troy (6 specimens
missing)

O. nitida ? Ford, Lansingburg

Kutorginalabradorica Bill,
Swanton Vt.

- 10

if

17

(1 type)
(1 type)

1bbl.

5667+1bbl. (278

36
46

types; 33 hypo-
types)

(1 type)
(1 type)

(3 hypotypes)

(6 hypotypes)

(3 hypotypes)

(4 hypotypes)

H. impar Ford,Troy

H. micans Bill., Troy |

Fordillatroyensis Barr., Troy

Aristozoe troyensis’ Ford,
Troy

Bathyurus senectus Bill. Bic

~ harbor Can. |

Microdiscus speciosus Ford,
Troy

Microdiscus speciosus Ford,
Lansingburg

M. meeki Ford, Troy

M. lobatus Hall, Troy

M. punctatus ? Salter, St John
N. B.

M. (sp.), Bic Harbor Can.

Olenellus asaphoides Em,
Troy

0. asaphoides Em., Bald moun-
tain

O. asaphoides Em., Lansingburg

O. vermontana Hall, Parker’s
farm, Vt.

0. thompsoni Hall, L’Anse-au-
Loup Can.

Ptychopdria teueer Bill., 4
mile east of Swanton Vt.

ae ae
eg plastotypes 1
Co., Rochester ra Bee ey.

Cumberland Md.

Total by purchase

-

Exchanges
andall, A. R., Alfred

Prephricaris horripilata
Clarke. |
a Cir incinnati society natural history, through
Dr Josua Lindahl
Phragmodictya eatilli-
formis. Keokuk beds, Crawfords-
ville Ind.

wa er eer inns. Helderbergian

Pa

426 (14 types; 36

hypotypes)

1 (1 type)

“Nautilus “Wise tes)
natus Hall. ‘Onondaga,

Kelleys Island O.— cae ik ue

Orthoceras casiveocs Hall,
Hamilton shales, Moravia

O. lima Hall. Hamilton shales,
Cazenovia aa

Gomphoceras pingue Hall.
Hamilton shales, north of Cazenovia

Orthoceras pertextum Hall.
Ithaca beds, Cornell-Fiske quarry,
Ithaca

GO. bebryx var. cayuga Hall.
Ithaca beds, Earl’s quarry, Ithaca

©. bebryx var. cayuga Hall.
Ithaca beds, University quarry,
Ithaca ,

O. bebryx var. cayuga, Cas-
eadilla ravine, Ithaca

Manticoceras sinuosus Hall.
Ithaca beds, University quarry,
Ithaca

Orthoceras anguis Hall.
Ithaca beds, Cascadilla creek,
Ithaca

O. fulgidum Hall. Ithaca beds,
Cascadilla creek, Ithaca

4

1
2 (2 hypotypes) —

3 (1 type)

1 (A. type)

7. Oe “Cox's ravine, Giearis Valley

_ wog, Lisle and vicinity

- Crustaceans from the Waterlime beds
at Wheelock’s farm, Litchfield

Fossils from the upper Ithaca and
Chemung rocks, Greene |

Fossils from the Portage rocks of
Naples and the Salina shales near
Pittsford

Guelph fossils from canal feeder, 2

a miles south of Shelby

Laforge, Laurence
Niagara fossils from Middleport
~~ Butts, Charles
; Remainder of fossils from the Che-

sheet, 1900

ss a ee the Ithaca beds, Killa-

mung and Carbonic rocks of Olean

225

1 420+1bbl.

100

300

90

70

300

2 400

*
anh: r, haiti a a

r Sela ay gh rei 7 he
. — Seen al, , ae :
, i)

Fossils from the Potsdam neti |
mantown horizons in ‘the: ake.’ aie a
Champlain basin : 400 — " “

Grabau, A. W. .

Fossils from limestone lenses in the
Clinton formation at Middleport

and Gasport : 300-
Van Deloo, Jacob ae

Euomphalus from the Chemung sand- Kea
) wif
stone near Union, Broome co. 13 Ee ai
: ahs. he - f
Total by collection 7 712+1bbl. ies.
ug :
Total accessions 13 829+2bbl. ae sie
types; 71 nYT
APPENDIX 2 types) oi ;

NEW ENTRIES ON GENERAL RECORD OF LOCALITIES
OF AMERICAN PALEOZOIC FOSSILS BELONGING TC
STATE MUSEUM : tatty

7 ALPHABETIC LIST OF LOCALITIES it (cay

Albany (North Albany), (Albany co.), 2565 ae

Alfred (Allegany co.), 2931 ry

Allegany (Cattaraugus co.), 2697, 2700, 2702, 2706, 2708, 2713, —
2720, 2723, 2724, 2727, 2728, 2733, 2865 re

Allen creek (Monroe co.), 3047, 3051 eee

Asbury (Tompkins co.), 2958, 2959 og

Ausable chasm (Clinton co.), 3031, 3032, 3033, 3034, 3035, 3036, .
3037, 3038, 3039, 3040, 3041, 3042, 3045
Avoca (Steuben co.), 2932

REPORT OF THD STATE PALEONTOLOGIST 1901 469

2 Bald mountain (Rensselaer co.), 2588

Barker run (Cattaraugus co.), 2885, 2886

R Becraft mountain (Columbia co.), 2696

_ Beehive creek (Cattaraugus co.), 3060

_ Beekmantown station (Clinton co.), 3044

_ Belknap’s gully (Yates co.), 3056

Bells gully (Canandaigua lake), 2908

Belmont (Allegany co.), 2735

Belvidere (Allegany co.), 2734

Bennetts hollow (Cattaraugus co.), 2712

Bice Harbor Can., 2592

Big Chazy river, 3025

Birch run (Cattaraugus co.), 2713

Boardman (Cattaraugus co.), 2855, 2856

Bolivar creek (Bradford co.), Pa., 2899

Boquet river, 3017, 3018

Bova creek (Cattaraugus co.), 3061, 3062, 3063

Bowler station (Allegany co.), 2781, 2868

Bozard hill (Cattaraugus co.), 2891

Branchport (Yates co.), 3056

Bredelar, Westphalia, Germany, 2917

Bristol Center (Ontario co.), 2906, 2929

Buffalo (Erie co.), 2568, 2577

Burdick (Chenango co.), 2545

Burdick’s crossing (Essex co.), 2999

Buttermilk falls (Tompkins co.), 2551, 2552

Camp Heart’s Content (Greene co.), 2977

Canandaigua (Ontario co.), 2936, 2946, 2950, 2951, 2954

Canandaigua lake, 2901, 2905, 2908, 2926, 2944

Carroll (Cattaraugus co.), 2780

Carrollton (Cattaraugus co.), 2862, 2898, 3064, 3065, 3066, 3067,
3068, 3089

Carrollton O., 2580

Cary hollow (Cattaraugus co.), 2697

Cascadilla creek (Tompkins co.), 2575

a ee Wy

hs oe

Chapin hill (Cetinrauieeth co cy 227, 2708
Chateaugay (Franklin co.), 3013, 3014
Chateaugay river, 3013 . .
Chazy (Clinton co.), 3006, 3008, 3009, 3010, 3011, “3012
Cherry Valley (Otsego co.), 2989 | fis +
Chipmunk creek (Cattaraugus « co.), 2698, 2699, 2720, 3070

3079, 3080, 3081 a |
Clarksville (Allegany co.), 2737, 2747, 2748, 2751, 24,3 DE

2761 a” nat
Clarksville Center (Allegany co.), 2738, 2739, 2743
Conesus lake, 2914 i
Coon hollow (Allegany co.), aie tele
Cooper’s hill (Cattaraugus co.), 2802, 2803, 2888, 2889, 2800 . " ;
Coopersville (Clinton co.), 3007, Sh ae
Corbeau creek (Clinton co.), 3007
Cowles hill (Chenango co.), 2527, 2528
Cox’s ravine (Otsego co.), 2989
Crown Point (Essex co.), 2999 =
Cuba (Allegany co.), 2747, 2748, 2750, 2751, 2752, 2754, 2767, 4 2758

2760, 2761, 2762, 2763, 2764, 2765, 2766, 2767, 2768, 2793, 79:

2795, 2798, 2805, 2806, 2872
Cumberland Md., 2949
Cummings crossing (Ontario co.), 3050

s .
*5e@ Pes

Dansville (Livingston co.), 2923

Day point (Clinton co.), 3053

Deer creek (Allegany co.), 2783
De Ruyter (Madison co0.), 2533, 2535, 2536, 2540, 2582

y glen (Tompkins co.), 2559, 2957 |
ek peecpicine co.), 2555, 2971, 2972, 2973, 2974, 2975, 2976

ea , guif (Chenango co.), 2529
t Rock point (Essex co.), 3019
nt creek (Ontario co.), 2903.
ae Forest Home (Tompkins co.), 2558
Prone Mile creek (Cattaraugus 235 2698, 2699, 2702, 2718, 2720,
2721, 2831, 2900 |
_ Fox’s point (Lake Erie), 2943
4 Friendship (Allegany co.), 2767, 2773
- Galt Ont., 2983, 2984, 2985, 2986, 2988
Geneva (Ontario co.), 2945
- Glenn (McKean co.), Pa., 2736
3 Glenwood (Tompkins co.), 2557
Glenwood Mont., 2581
_ Grant Hollow (Rensselaer co.), 2982
_ Great Valley (Cattaraugus co.), 2878, 2879, 2881, 3091
_ Great Valley creek (Cattaraugus co.), 2878, 2879, 3090
_ Greene (Chenango co.), 2527, 2528, 2529, 2530
_ Grimes gully, Naples (Ontario co.), 2934
Groton (Tompkins co.), 2978, 2979, 2980
Gull berg (Ontario co.), 2927
_ Gull brook (Cattaraugus co.), 2785, 2864
Hackberry Grove, Ia., 2694

Havana glen (Gehuyler co), 2 ol aS

Hespeler Ont., 2987 ai ee = |

Highgate Vt., 2594 ae |

High point (Ontario co.), 2935

Himrod (Yates co.), 3055

Hinsdale (Cattaraugus co.), 2784, 2785, 2786, 289, 2
2870, 2871

ony

Hollow brook (Cayuga co.), 2981 Oe ae 4
Honeoye lake, 2913 ek Ma
Humphrey Center (Cattaraugus co.), 2801, 2802, 2892 By ks ie
Hungry hollow (Cattaraugus co.), 3092 ae

Idar, Germany, 105 (yellow ticket)
Independence Ia., 2695

Indian creek (McKean co.), Pa. 2772, 2867
Irish brook (Cattaraugus co.), 3072, 3073, 3074

Irvine Mills (Cattaraugus co.), 3071 ie hes Is
Ischua (Cattaraugus co.), 2774, 2807, 2808, 2809, 2810, 2811, 2812,

2813, 2815, 2816, 2818, 2864, 2871, 2874 oF oe
Ischua creek (Cattaraugus co.), 2818 oye
Island of Oesel, Livonia, Russia 107 (yellow ticket) 2
Ithaca (Tompkins co.), 2547, 2548, 2549, 2550, 2551, 2552, 2554,

2555, 2556, 2572, 2578, 2574, 2575, 2576, 2971, 2972, 2973, 2974, ©

2975, 2976
Ithaca falls (Tompkins co.), 2971, 2972
Java Village (Wyoming co.), 2939
Juliand hill (Chenango co.), 2530
Katzenloch near Idar, Germany, 105 (yellow ticket)
Kelleys Island O., 2569
Kent’s falls (Clinton co.), 3000, 3001, 3002, 3022, 3023

<1

REPORT OF THE STATH PALEONTOLOGIST 1901

Killbuck (Cattaraugus co.), 2882, 2883, 3085, 3090

Kirkwood (Broome co.), 2993

Knapp Creek (Cattaraugus co.), 2701, 2702, 2719, 2732, 2900
Knapp hill (Ontario co.), 3049

Lake Champlain, 3016, 3018, 3043

Lake Erie, 2568

L’Anse-au-Loup Can., 2596

Lansingburg (Rensselaer co.), 2587, 2588

Laphams Mills (Clinton co.), 3021

Laurens (Otsego co.), 2531

Lawrence station (Greene co.), 2977

Learn hill (Cattaraugus co.), 2817

Lime Creek Ia., 2694

Limestone (Cattaraugus co.), 2896

Limestone brook (Cattaraugus co.), 2895, 2896, 2897
Lincoln gaily (Ontario co.), 3046

Litchfield (Herkimer co.), 2579, 2583

Little Ausable river, 3004

‘Little Genesee (Allegany co.), 2782, 2869

Little Valley (Cattaraugus co.), 2876

Locke (Cayuga co.), 2981

Lockport (Niagara co.), 2585

Lodi falls (Seneca co.), 2940

Louds creek (Cattaraugus co.), 2847

Louds creek (McKean co.) Pa., 2770
Ludlowville (Tompkins co.), 2566, 2961, 2962
McIntosh creek (Cattaraugus co.), 3078

473

McKinney’s (Tompkins co.), 2560, 2561, 2562, 2568, 2564, 2955,

2956, 2960, 2964, 2965, 2966, 2967

Manlius (Onondaga co.), 2693

Marble river, 3013, 3014 -

Melrose (Rensselaer co.), 2982

Mooers (Clinton co.), 3026

Moravia (Cayuga co.), 2570

Mount Hermon (Cattaraugus co.), 2828, 2824, 2825
2841

2826,

2821,

** 2717, 2718, 2721, 2784, 2821, 2822, 2824, 2825, 2827,

\

Newton run pai Be o.), 28 2875, 30%
Nine Mile creek (Cattaraugus £0), 2 = 24 , 8
North Cuba (Allegany co.), 2758 be.
Oil creek (Cattaraugus co.), 2795, 2796, 2798, 2806

Olean (Cattaraugus co.), 2704, 2705, 2706, 2709, min?

he ie

2800, 2802, 2893, 2884, 2895, 2897, IRBS, 2900, 284, 2
2844, 2845, 2846, 2848, 2850, 2851

Orwell Vt., 3016

Oswayo creek (Cattaraugus co.), 2861

Ouaquaga (Broome co.), 2995

Oxford (Chenango co.), 2938

Parrish gully (Ontario co.), 2910

Peruville (Tompkins co.), 2553

Peth (Cattaraugus co.), 2884»

Pitcher mineral springs ravine (Chenango co.), 2541

Pittsford (Monroe co.), 2952, 3047, 3051, 3052

Plattsburg (Clinton co.), 2998, 3000, 3001, 3003, 3022, 3030

Plumb creek (Yates co.), 83055

Pontiac (Erie co.), 2942

Port Kent (Essex co.), 3043

Portland (Tompkins co.), 2958, 2959, 2963 +

Portville (Cattaraugus co.), 2740, 2770, 2771, 2852, 2853, 2859,
2860, 2861, 2863 Be

Poughkeepsie (Dutchess co.), 2590

Prattsburg (Steuben co.), 2933

Pumpkin hollow (Cattaraugus co.), 2726 |

Red House creek (Cattaraugus co.), 3061, 3062, 3063, 3075, 3076

Renwick creek (Tompkins co.), 2968, 2969, 2970

36, 3087, 3088, 3092, 3093

eer (Fanpkins co,); 2566, 2961, 2962,
ul river, 3020 |
€ river, 3000, 3001, 3002, 3003, 3022, 3023, 3030
rie (Schoharie co.), 2990
uyler Falls (Clinton co.), 3004 ;
tt (Cattaraugus co.), 2791, 2800
_ Shelby (Orleans co.), 2996
‘Siegen, Germany, 106 (yellow ticket)

=-2544, 2546

- South Plattsburg (Clinton co.), 3020

_ Spafford (Onondaga co.), 3054

_ Stafford (Genesee co.), 2567, 2904

% Stony point (Erie co.), 2991

_ Sugartown (Cattaraugus co.), 2887, 3069

} - Swanton WV t27 2591

q Ticonderoga (Essex co.), 3015, 3027, 3028, 3029
_ Ticonderoga creek (Essex co.), 3015, 3029

: _ Tracy Creek (Broome co.), 2994 -
_ Trenton Falls (Oneida co.), 2578

B Triphammer falls (Tompkins co.), 2555

_ Troy (Rensselaer co.), 2586

_ una creek (Cattaraugus co.), 3070, 3071, 3072, 3079, 3080, 3081
_ Tuna Valley (Cattaraugus co.), 3084
Two Mile creek (Cattaraugus co.), 2718
Union (Broome co.), 2992
Valcour station (Clinton co.), 2997, 3053

_

We ietets co.), 2875, 2898, 3057, 3058, 3059, 3077,

South Otselic (Chenango co.), 2534, 2536, 2538, 2539, 2542, 2543,

; fs West hill one ae

West Seneca (Erie pe, ine ane ) ee
Westons Mills (Cattaraugus co.), 2867 <> ee
Wildcat creek (Cattaraugus co.), 2829 =
Wildcat hollow (Cattaraugus co.), 2828, 2842
- Willsboro (Essex co.), 3017, 3018, 3019
Windfall creek (Allegany co.), 2782

Wing hollow (Cattaraugus co.), 2707, 2708, 2710
Wolf creek (Allegany co.), 2740, 2741, 2744, 2745, 2746 As
Wolf run (Cattaraugus co.), 2742, 2746, 2854, 2858 oo 8 -
Woodchuck hollow (Cattaraugus co.), ase: 2849 ca “oa
Woodville (Ontario co.), 2925 . ae E a | ag

NEW YORK LOCALITIES ACCORDING TO COUNTIES

(Names in italic are new to the record. )

Albany co. Allegany co. (continued)
Albany Dodge creek
North Albany Friendship
Allegany co. Little Genesee
Alfred North Cuba
Belmont Van Campens creek
Belvidere Wellsville
Bowler station Windfall creek
Ceres Wolf creek
Clarksville Broome co.
Clarksville Center Kirkwood
Coon hollow Ouaquaga
Cuba Tracy Creek

Deer creek Union

ea Ellicottville
Fay hollow
ss PPive Mile creek

Be Four Mile creek
Great Valley

Gull brook
Halls
- Harrisburg
Haskell creek
Haskell Flats
Hinsdale
Humphrey Center
Hungry hollow
Irish brook
Ervine Mills
Ischua
Ischwa creek

Nine Mile creek

Great Valley creek |

Oil creek
Olean

Oswayo creek
Peth —
Portville
Pumpkin hollow
Red House creek

Rice brook

Riverside junction
Rock City
Russell station
Salamanca
Scott |
Sugartown
Tuna creek
Tuna Valley
Two Mile creek
Vandalia
Wayman branch
Westons Mills
Wildcat creek
Wildcat hollow

Juliand hill
Oxford

Pitcher mineral springs

ravine
South Otselic

West [Willard’s] hill
Clinton co. -

Ausable chasm

Beekmantown station $ Genesee co.

Champlain
Chazy
Coopersville
Corbeau creck
Day point
Kent's falls
LIaphams Mills
Mooers
Plattsburg
Schuyler Falls
South Plattsburg

Greene co. ae :
Camp Heart's Content a
Lawrence station |

Herkimer co.

Dolgeville
Litchfield
Livingston co. 3

Cashaqua creek

“a

Dansville
Mount Morris

papi

ates Scio
Havana glen
Seneca co.
Lodi falls
Steuben co.
‘fl Ayoeca
Cummings crossing Prattsburg |
‘Flint aoe a eames Tomplans co.
fp Geneva | } Asbury
Grimes gully (Naples) Buttermilk falls
Gull berg : Cascadilla creek
Hatch hill | Esty glen
High point Fall creek
Knapphill | Forest Home
Lincoln gully Glenwood
Naples Groton
Parrish gully ithaca. ™.
West hill | Ithaca falls
ae Woodville Ludlowville
Orleans co. | McKinney's
Shelby Peruville
Otsego co. Portland
Cherry Valley Renwick creek

Cox's ravine Salmon creek

are
Sst Se
ks
- Ee

ao

yee ies pi
es Java Village | | |

INDEX TO FORMATIONS: SR

eieveiiae (Greyson shales), 2581 gis. pie

Cambric, 2586, be 2588, 2589, 2590, awl, 2592, 2598, 28
2596.

Potsdam sandstone, 3000, 3001, 3002, 3004, 3006, ~—
3010, 3011, 3012, 3014, 3015, 3016, 3019, 3022, 3023, 2¢
3027, 3028, 3029, 3031, 3032, 3038, 3034, 3035, 3036, 3087, +3038
3039, 3040, 3041, 3042, 3045. a ‘ di

Beekmantown limestone, 2982, 2999, 3006, 3009, 3010, 3011, § 012,
30138, 3015, 3016, 3017, 3018, 3020, 3025, 3027, 3028, 3029, é eo:

Chazy limestone, 2997, 2998, 3003, 3005, 3024, 3043, 3053. ee

Trenton limestone, 2578, 3030. ee
Utica slate, 2565, 2947. ag
Niagara beds, 2585. : cay ee % he
Guelph formation, 2953, 2983, 2984, 2985, 2986, 2987, 2088, 2996, ;
Salina beds, 2952, 2968, 3052. Eat
Rondout waterlime, 2577, 2579, 2583, 2950. Ce

Devonic, 2694, 2695, 2917.

Helderbergian, 2584, 2919, 2948, 2949, 2968.

Oriskany beds, 2696, 2968,

Onondaga limestone, 2567, 2568, 2569, 2918, 2968.

Marcellus shale, 2693, 2903, 2904, 2936, 2945, 2954, 2968, 2989,

2990, 2991. '

Agoniatites limestone, 2693, 2990.
Stafford limestone, 2904.

Hamilton beds, 2570, 2571, 2901, 2902, 2951, 2968.

Tully limestone, 2531, 2532, 2582, 2968.

Na Pes ned 2909, 2910, 2911, 2912, 2913, 2914, 2915, 2920,
33 2921, 2922, 2923, 2930, 2939, 2942, 2943, 2944, 3055, 3056.
_ Wiscoy beds, 2924.
‘Ithaca beds, 2526, 2527, 2528, 2530, 2538, 2534, 2535, 2536,
a z -:2537, 2588, 2589, 2540, 2541, 2542, 2543, 2544, 2545, 2546,
& —s- 2547, 2548, 2549, 2550, 2551, 2552, 2553, 2554, 2555, 2556,
ss, 2558, 2560, 2561, 2562, 2563, 2564, 2572, 2573, 2574,
_-——s—ss«O'T5, 2576, 2582, 2934, 2955, 2956, 2960, 2961, 2963, 2964,
——s—s«2965, 2966, 2967, 2968, 2969, 2970, 2971, 2972, 2973, 2974,
-—s- 2975, 2976, 2978, 2979, 2980, 2981, 3054.
: _ Oneonta, 2938, 2977. |
Chemung beds, 2529, 2697, 2705, 2706, 2709, 2710, 2711, 2714, 2715,
i 2720, 2721, 2723, 2724, 2726, 2727, 2728, 2729, 2733, 2734, 2735,
2737, 2738, 2748, 2748, 2752, 2755, 2756, 2757, 2758, 2759, 2760,
2761, 2762, 2763, 2764, 2765, 2767, 2768, 2770, 2771, 2772, 2773,
- —«- BTTA, 2775, 2776, 2780, 2781, 2782, 2783, 2784, 2785, 2786, 2787,
2788, 2789, 2790, 2791, 2792, 2793, 2794, 2795, 2796, 2797, 2798,
2800, 2801, 2802, 2804, 2805, 2806, 2807, 2808, 2809, 2810, 2811,
2812, 2813, 2814, 2815, 2816, 2818, 2819, 2820, 2821, 2822, 2829,
«2833, 2837, 2839, 2842, 2848, 2844, 2845, 2846, 2848, 2849, 2850,
4 2851, 2852, 2854, 2855, 2856, 2857, 2858, 2859, 2861, 2863, 2864,
3 2866, 2867, 2868, 2869, 2870, 2871, 2872, 2873, 2874, 2876, 2877,
_ __- 2878, 2879, 2881, 2882, 2883, 2884, 2885, 2887, 2888, 2889, 2890,
| 2891, 2892, 2893, 2896, 2916, 2931, 2932, 2938, 2935, 2937, 2946,
2992, 2993, 2994, 2995, 3046, 3049, 3050, 3057, 3060, 3061, 3062,
3063, 3064, 3065, 3066, 3069, 3070, 3072, 3076, 3078, 3081, 3082,
3083, 3084, 3085, 3086, 3087, 3088, 3089, 3090, 3091, 3092, 3093.
Lower Carbonic, 2697, 2698, 2699, 2700, 2701, 2702, 2703, 2704,
27072708, 2712, 2713, 2716, 2717, 2718, 2719, 2722, 2725, 2726,
2729, 2730, 2731, 2732, 2736, 2739, 2740, 2741, 2742, 2
2747, 2749, 2750, 2751, 2753, 2754, 2766, 2769, 2771, 2
| 2779, 2801, 2803, 2817, 2823, 2824, 2825, 2826, 2827, 2

= ia:

2528

2529

2530

2531

— 2532

2533

2534

hate collector. 1900. By | e
Ithaca beds. West, or Willard’s, aa, a need
Greene, and } mile north of Cowles hill. DI
collector. 1900. ees Bae:
Chemung beds. Flagg gulf, lower part, Greene,
Luther, collector. 1900. te es
Ithaca beds. Juliand hill, Greene. D. D. Luther, ¢
tor. , 1900. — t o ea ig
Tully horizon. Laurens, Otsego co.; small ravine w of
village. D. D. Luther, collector. 1900. . 3 : : =
Tully horizon. 1 mile southwest of New Lisbon [N =
ville], Otsego co. D. D. Luther, collector. ite bidet hes
Ithaca beds. Loose near top of hill southeast of 1] y 7
Ruyter, Madison co. ©. 8. Prosser, collector. ( 390)
1901. Nia
Ithaca beds. 3 miles east of South Otselic, Chenango oa.
and in glen below the “ upper reservoir ”; Priest’s farm. —
CO. S. Prosser, collector. (1895) 1901. es
Ithaca beds (Sherburne). In glen southeast of De Raytie: ‘a
C. 8S. Prosser, collector. (1895) 1901.

Ithaca beds. Lower part of glen east of South Otselic.
C. 8. Prosser, collector. (1895) 1901.

Ithaca beds. Loose in Havana glen, Schuyler co, ©. S.
Prosser, collector. (1895) 1901.

Ithaca beds. Shales in lower part of glen east of South
Otselic. C. 8. Prosser, collector. (1895) 1901.

Ithaca beds. Glen east of South Otselic; above the “lower
reservoir.” OC. S8. Prosser, collector. (1895) 1901.

— 2541
2542.
25438
2544

2546

2550

2551

REPORT OF THE STATE PALEONTOLOGIST 1901 483

| Ithaca beds. Burdick quarry on hill 14 miles southeast of

De Ruyter and 324 feet above the village. C.S. Prosser,
collector. (1895) 1901.

Ithaca beds. Lower part of Pitcher mineral springs
ravine, Chenango co. C.S. Prosser, collector. (1895)
1901. :

Ithaca beds. Shaly sandstone and shales with base of
North Norwich fauna, in glen east of South Otselic.
C. S. Prosser, collector. (1895) 1901.

Ithaca beds. In glen east of South Otselic from roadside
below the “ lower reservoir.” CC. 8. Prosser, collector.
(1895) 1901.

Ithaca beds. Glen east of South Otselic; Tropido-
leptus zone at second bridge. C. S. Prosser, col-
lector. (1895) 1901.

Ithaca beds. On roadside east of Burdick, Chenango co.;
Portage barren shales with part of the Sp. mucron-
atus (Ithaca) fauna. C.S. Prosser, collector. (1895)
1901.

Ithaca beds. Glen east of South Otselic; above Tropi-
doleptus zone. C. S. Prosser, collector. (1895)
1901. ;

Ithaca beds. Driscoll’s quarry east of State st., Ithaca.
C. A. Hartnagel and H.S. Mattimore, collectors. 1901.

Ithaca beds. South Cayuga st., Ithaca. C. A. Hartnagel
and H. 8S. Mattimore, collectors. 1901.

Ithaca beds. Fowler’s quarry south of Ithaca along
Delaware, Lackawanna and Western railroad, just
beyond 2550. C. A. Hartnagel and H. 8S. Mattimore,

collectors. 1901.

Ithaca beds. Sheehy’s quarry, Ithaca; first quarry south
of Ithaca along Delaware, Lackawanna and Western
railroad. C. A. Hartnagel and H. S. Mattimore, col-
lectors. 1901.

Ithaca beds. Foot of Buttermilk falls, Ithaca. ©. A.
Hartnagel and H. S. Mattimore, collectors. 1901.

2556

2557

2558

2559

2560

2562

2563

- Hartnagel and H. ‘'S. Matt
2555 Ithaca beds. Foot of. Triphammer |

-hights, Ithaca;

Ithaca. ©. A. Hartnagel and H. 5 Ma ae re
lectors. 1901.
Ithaca beds: Bates quarry alone Delawaterk LC
and Western railroad tracks on hill south of ha o
C. A. Hartnagel and H. 8. Mattimore, collect Oana
Ithaca beds. Glenwood, Tompkins co.; along «
mile from Cayuga lake. C. A. Hartnagel and 1
Mattimore, collectors. 1901. |

Ithaca beds. Below mill dam, Forest Home, Tdmpkh
co. ©. A. Hartnagel and H. 8. Mattimore, cers eo
1901. ben

Lower Portage beds. 1 mile below Esty glen, Cayuga
lake (Tompkins co.), along railroad. ©. A. Hartnagel —
and H. 8. Mattimore, collectors. 1901. = ¥e et

Ithaca beds. South glen at McKinney’s, Cayuga lake, 50
yards above 2956. C. A. Hartnagel and H. §. Matti- “a j
more, collectors. 1901. :

Ithaca beds. North glen at McKinney’s, Cayuga lake; -
20 feet above lake. C, A. Hartnagel and H. 8. Matti- —
more, collectors. 1901.

Ithaca beds. North glen at McKinney’s, Cayuga lake
second falls, 130 feet above lake. C. A. Hartnagel and ~
H. 8. Mattimore, collectors. 1901. i

Ithaca beds. North glen at McKinney’s, Cayuga lake;
short distance above 2955. C. A. Hartnagel and H. 8.
Mattimore, collectors. 1901.

tage

2580

REPORT OF THE STATE PALEONTOLOGIST 1901 485

Ithaca beds. South glen at McKinney’s, Cayuga lake, 50 ©
yards above 2960. C. A. Hartnagel and H. S. Matti-
more, collectors. 1901.

Utica horizon. Felt mill, city line (North Albany) Al-

_bany. H.S. Mattimore, collector. 1901.

Genesee shale. Right branch of Salmon creek, 24 miles
northeast of Ludlowville, Tompkins co. 540 feet A. T.

Onondaga limestone. Stafford, Genesee co. C.K. Swartz,
donor.

Onondaga limestone. Bottom of Lake Erie at Buffalo.
W.P. Judson, donor. 1901.

Onondaga limestone. Kelleys Island O. H. P. Cushing,
Cleveland O., exchange. 1901.

Hamilton beds. Moravia, Cayuga co. H. P. Cushing,
exchange. 1901.

Hamilton beds. Cazenovia, Madison co. H. P. Cushing,
exchange. 1901.

Ithaca beds. Cornell-Fiske quarry, Ithaca. H. P. Cush-
ing, exchange. 1901.

Ithaca beds. Earl’s quarry, Ithaca. H. P. Cushing, ex-
change. 1901.

Ithaca beds. University quarry, Ithaca. H. P. Cushing,
exchange. 1901.

Ithaca beds. Cascadilla creek, Ithaca. H: P. Cushing,
exchange. 1901. y

Ithaca beds. Cascadilla quarry, Ithaca. H. P. Cushing,
exchange. 1901.

Waterlime; Eurypterus. beds. Buffalo cement ¢co0.’s
quarry, Buffalo. L. J. Bennett, donor. 1901.

Trenton limestone. Trenton Falls, Oneida co. Ward &
Howell purchase. 1901.

Waterlime; Eurypterus beds. Litchfield, Herkimer co.
Ward & Howell purchase. 1901.

Lower barren Coal Measures. Carrolton O. J. M.

Clarke, donor. 1900.

2590.

2591

2592

2593

- 2594

2595

2596

-Helderbergian. Herkimer co. Ward & Howell purcha
‘ a ie

Cambric. Near Swanton Vt. S. W. Ford collection, par

cemetery, De taster,
‘lector. 1895.0 ;
Waterlime. Litchfield, Herkimer 0.3 small out

Alger farm next east of the Wheelock

‘adisc 1é 4
ete it eet ie
,

. % we) ’
* ee

Luther, collector. 1900.

1900.

Niagara limestone. Lockport, Niagara co.
Howell purchase. 1900. |
Cambric. Troy, Rensselaer co. S. W. Ford
purchased. 1900. |
Cambric. Lansingburg, Rensselaer co. . Ww Ford « 20l- es
lection, purchased. 1900. ae
Cambric. Bald mountain, near Lansingburg. 8 We:
Ford collection, purchased. 1900. o ee

Cambric. Reynold’s Inn, Washington co. 8. W. Ford
collection, purchased. 1900. 4

Cambric. Poughkeepsie. §. W. Ford collection, pure
chased? 1900.

>» sag

i 4
. wr
or

‘

chased. 1900. ae

Cambric. Bic Harbor Can. 8S. W. Ford collection, pur: i
chased. 1900.

Cambric. St John N. B. S. W. Ford collection, pur-
chased. 1900.

Cambric. Highgate Vt. 8S. W. Ford collection, pur-
chased. 1900.

Cambric. Parker’s farm Vt. 8S. W. Ford collection, pur-
chased. 1900.

Cambric. L’Anse-au-Loup Can. S. W. Ford collection,
purchased. 1900.

REPORT OF THE STATE PALBONTOLOGIST 1901 487

Marcellus (Agoniatite) limestone. Manlius, Onondaga
co. John D. Wilson, Syracuse, donor.

Upper Devonic. Hackberry Grove, Lime Creek Ia.
Samuel Calvin, donor. 1901.

Upper Devonic. Independence Ia. Samuel Calvin, donor.
1901.

Oriskany. beds. Becraft mountain, Columbia co. J. M.
Clarke, C. E. Beecher, C. Schuchert and M. Sheehy, col-
lectors. .

Fossils collected by Charles Butts in area covered by the
Olean quadrangle, Cattaraugus county, 1900. The horizons of
this area are numbered as follows, beginning at the top. Local-

ity numbers 2697-2863 inclusive.
1 Arenaceous shales above the Olean conglomerate 15 feet

2 Olean conglomerate : 60 feet
3 Interbedded shales and sandstones with Camaro-

toechia allegania Williams 150 feet
4 Impure limestone - 45 feet
5 Barren shales and sandstones 100 feet
6 Mount Hermon sandstones . 10 feet
7 Interbedded red and green shales and flaggy and

shaly arenaceous sandstones 220 feet
8 Wolf creek conglomerate 10 feet
9 Green shales and thin bedded arenaceous sand-

stones E 130 feet
10 Chocolate shales and purplish sandstones; upper

limit of Athyris angelica 100 feet
11 Shales and sandstones | 75 feet
12 Shales and arenaceous sandstones with abundance

of Orthothetes chemungensis 160 feet
13 Cuba sandstone 10-15 feet

Thicknesses as here given are only approximate. Numbers
referring to these horizons are recorded with the following
entriés:

2697 Ravine south from near head of Cary hollow, 2 miles
southwest of Allegany, Cattaraugus co. 1675 feet and

2701

2702

2703

2704

South side of high hin 4:40 5 5 miles south ve
; ae

no. 3.

gany. 2100 feet A. T., no. 3. hae

Loose near top of hill 4 mile north of Kapp ¢
2330 feet A. T., no. 3.

Road just east of Knapp Creek and road —
Creek down Four Mile creek to Allegany. ia ] 238
feet A. T., no. 3; [A 90] 2300 feet A. T., no. 3; 2150 fe eet
and 2130 feet A. T., no. 4; 1850 feet A. T., no. 1 “
feet A. T. horizon? | es ye

Old, washed-out road south of Rock City and just nort th FE
of New York-Pennsylvania boundary. 1830 feet A. bos
no. 7; 1820 feet A. T., no. 7. i

Loose; cut from layer of shale in place at summit above a

conglomerate at Rock City, southwest of Olean. 2360
feet A. T., no. 3. * em

Old quarry on road between Olean and Five Mile ae ce
miles northwest of Olean. 1590 feet A. T., no. 10.

Pit on top of hill ? mile east of junction of Five Mile, Alle- - 4
gany and Olean roads. 1810 feet A. T., no. 9. :

South of Wing hollow, 1 mile west of Five Mile road,
Allegany township. 2000 feet A. T. (loose), no. 6.

Eastern spur of high hill at head of Wing hollow, 4 miles ©
northwest of Allegany. 1960 feet and 1710 feet A. T.
(loose), no. 6. :

Cut in Olean, Rock City and Bradford trolley line, about
2 miles southwest of Olean. 1640 feet A. T., no. 10.

Eastern spur of high hill at head of Wing hollow in angle
between Wing hollow and Five Mile road. 1800 feet
A. Day. 0. @: , yy

2715

2716

2717

2718

2719

2720

2721

2722

2723

2724

2725

REPORT OF THE STATE PALEONTOLOGIST 1901 489

Blind road near Olean-Allegany township boundary, 3
miles northwest of Olean. 1880 feet and 1910 feet
AT, 10.-9:

Top of ridge between Olean and Bennett’s hollow near
Olean-Allegany township boundary, 3 miles northwest
of Olean. 1930 feet and 2030 feet A. T. (loose), 1965
feet A. T., no. 8.

Near head of southeast branch of Birch run, southwest
of Allegany. 1840 feet, 2015-25 feet A. T. (loose), no. 6.

On hillside above trolley road, 24 miles southwest of
Olean. 1600 feet A. T. (loose), no. 9?

4 mile east of Erie R. R. depot, Vandalia. 1440 feet A. T.,
mendes <2 |

State line by Olean, Rock City and Bradford trolley road.
2300 feet A. T., no. 3.

Loose; trolley road about 4 miles southwest of Olean.
1760-1800 feet A. T., no. 8.

Crest of ridge between Two Mile and Four Mile creeks,
about 4 miles southwest of Olean. 1890 feet A. T.,
no. 7.

Cut on Olean, Rock City and Bradford trolley road be-
tween state line and Knapp Creek. 2315 feet A. T,,
no. 3.

South of road between Four Mile and Chipmunk creeks,
34 miles southwest of Allegany. 1770 feet A. T., no. 9.

Along Four Mile creek about 4 miles southwest of Olean.
1560 feet A. T., no. 9.

West side of northwest spur of Rock City hill. 1985 feet
fe nb. 0,

Four Mile road near where road to Rock City branches off,
4—5 miles south of Allegany. 1725 feet A. T., no. 9.

Road between Nine Mile and Five Mile creeks, about 54
miles northwest of Allegany. 1685 feet A. T., no. 11.

1-2 miles northeast of Harrisburg, 3 miles north of New
York-Pennsylvania boundary line. 2820 feet A. T.,
no. 3.

2730

" West side of Mt Moriah. {A ant)" 2060 feet A 2 "3 F

1800 feet A. T., ner 1880 feet !

Summit of northeastern spur of Mt Mor
south of Russell station, Pennsylvania R [.
1630 feet A. T., no. 9, [A 2514] 1940 feet AT

West side of Mt Moriah $ mile south of Russ ell
on Pennsylvania R. R. 2140 feet A. T., (loose) I rizo
[A 252] 2140 feet A. T. loose? [A 2521] a ot A
no. 6.

[A 2523] 2030 feet A. T., no. 7. aoe
Road forking at state line south of Knapp Creek. 230 ae
feet A. T. (loose), no. 3. | =

End of blind road 34 miles northwest of Allege wg!
[A 257] 1850 feet A. T. (loose), no. 9,? [A 258®4] 2 )0-
1860 feet A. T. (loose), no. 9? a

Bed of Van Campen’s creek just above railroad bridge,
Belyidere, Amity township, Allegany co. 1400 feet
A. T. Below Cuba sandstone.

Quarry near Belmont cemetery; loose stone on roadside -
4 mile southwest of Belmont. 1470 feet A. T. Below :
Cuba sandstone. a a

West of Glenn postoffice, McKean co. Pa. at 2190 feet; :
road forking. 2100-2190 feet A. T., no. 4? 4

Ravine 1 mile southwest of Clarksville, Allegany co. west
of highway. 1650-1700 feet A. T., no. 12. ;

Loose near head of ravine on east side of highway about q
} mile south of Clarksville Center, Allegany co. [Cl. 21] p.
1650-1800 feet A. T. [Cl. 22] 1770-1795 feet A. T., no. 12.

oo

=

REPORT OF THE STATE PALEONTOLOGIST 1901 _ 49t

mile south of Clarksville Center. 2000 feet A. T., no. 7? ©
2740 Loose east side of Wolf creek near Joel Wixon’s farm
about 6 miles northeast of Portville. 1800 feet A. 2 iy
no. 8. Collection from boulders horizon of conglomer-
: ate 50-75 feet higher.
2741 Loose on hillside east of Wolf creek about 14 miles north
} of junction with Dodge’s creek. 1950 feet A. T., no. 7.
2742 Road ditch near head of Wolf run. 2160 feet A. T., no. T.
2743 Ravine on hillside $ mile due north of Clarksville Center.
1710 feet A. T., no. 9.
2744 West side of Wolf creek, steep escarpment west of wide
flat in valley bottom 5 miles northeast of Portville.
1890 feet and 1895 feet A. T., no. 8; 2225 feet A. T., no. 3.
2745 Road on Wolf creek about 7 miles northeast of Portville.
1875 feet A. T. (loose), horizon?
-2746 Summit of hill, given as 2378 feet on Olean quadrangle,
between Wolf creek and Wolf run. 23860 feet A. T.,
no. 3.
2747 Summit on Cuba-Clarksville road, Clarksville township.
2050 feet A. T. (loose), no. 8.
2748 Roadside cut Cuba-Clarksville road in Clarksville town-
ship; also loose on summit of road. 1850 feet A. T.,

J
;
~-,
‘a

2

4

d

2,

no. 9.

2749 Southwestern part of Clarksville township. 2000 feet
A T., ne.-8.

2750 Top of hill about 4 miles nearly due south of Cuba and just
south of Cuba-Clarksville boundary. 2122 feet A. T.,
no. 7.

2751 Bank of creek on Cuba-Clarksville road near third road
forking south of Cuba. 2020 feet A. T. (loose), no. 8?

2752 Ravine east of Cuba-Haskell road just south of Cuba-
Clarksville boundary. [Cl. 160] and [Cl. 1607] 1710 feet

~ and 1795 feet A. T., no. 11; [Cl]. 1603] ?, [Cl. 16048] 1810-

60 feet A. T., no. 10.

2760

2767

Ravine 3 miles south of Cuba on road brane!

ash
yrs 2

junetion with: ) Haskell pad. 1
Glarkeville ie 1755 feet - , no. 11.
Armstrong quarry near Erie depot, Cuba. 5
Ravine on east side of hill west of road to: |
mile north of Cuba village. 1700 feet A. n, er
From 2-3 miles east of west county line, 4
north of Cuba-Clarksyille boundary. 1960 feet :
no. ® Sl) Sera) en
second road to left from Clarksville-Cuba’ ae going
south. [Cu 15612] 1785, 1760 and 1735 feet at no.
11. [Cu 156 * © *] 1855 and 1875 feet A. T., no. 10; [Cu
156°] 1925 feet A. T., no. 9. 4 ae
Ravine on west side of Cuba-Clarksville road, 3 miles south
of Cuba. 1760 feet A. T., no. 11. ; a
Along stream about 3$ miles southwest of Cuba. 1675 feet
A. T., no. 11. 3 ma
Ravine in southwest corner of Cuba township, 3 = 3
southwest of Cuba. 1705 feet A. T., no. 12. “ae
Creek bank } mile west of Cuba reservoir just west of —
county line; 1590 feet A. T., no. 18.
Ravine 2 miles southeast of Cuba. 1732 feet A. T., no. 11. — q
Field in elbow of road 23 miles southeast of Cuba village;
also loose in vicinity of high hill from 1-2 miles north _
of Cuba-Clarksville boundary. [Cu 185] 1900 feet A.T. —
(loose), no. 8; [Cu. 186'] 2115 feet A. T., no. 8.
Road up hill from summit between Cuba and Friendship,

-

Allegany co. in southwesterly direction in southern cen-
tral part of Cuba township. 1790, 1860, 1870 feet A. T.,

no. 1)?

REPORT OF THE STATE PALEBONTOLOGIST 1901 493

Ravine on west side of valley 2 mile south of Cuba. 1560,
1570, 1585, 1600, 1635 feet A. T., no. 12; 1750, 1790, 1800
feet A. T., no. 11.

River flats west of Bullis’s mill near state line, Eldred
township, McKean co. Pa. 1415 feet A. T. (boulders),
no. 8. Position?

Road banks Portville-Eldred road 4 mile east of intersec-
tion of Louds creek, Eldred township, McKean co. Pa.
1415 feet A. T., no. 9.

Roadside cut on Portville-Eldred road, near river, about 7
miles from Portville in Eldred township, McKean co. Pa.
[E 98] 1425 feet A. T., no. 9; [E 98'] 1425 feet A. T.

(loose), no. 8.

2772 Shale bank by roadside 1 mile north of Eldred Pa. near
mouth of Indian creek. 1450 feet A. T., no. 9.

2773 Roadside ditch of road southeastern corner of Friendship,

; Allegany co. between lots 2 and 3. 2075 feet A. T., no.

9?

2774 Ravine entering Ischua valley from northeast, in south-
eastern corner of Franklinville township. 1750 feet
A. T., no. 12.

2775 Road over high hill in southeastern part of Franklinville
township; east side. [F 202] 1780 feet A. T., no. 12;
[EF 2024] 1995 feet A: T., no. 10; [ 2022+] 2030, 2100,
2150 feet A. T., no. 9.

2776 Road running due east and west 4 mile north of Hum-
phrey-Franklinville boundary, southeastern part of
Franklinville township. 22385 feet A. T., no. 9.

2777 Southeastern corner of Friendship township. 2235 feet
8. 110... 97.

2778 Field on top of high hill in angle formed by roads in mid-
dle of southern part of Franklinville township on lot 17,
4 mile north of Franklinville-Humphrey boundary. 2250
feet A. T., no. 8.

2779 Loose; crest of ridge, Rock City, Genesee township, short
distance west of rocks. 2310 feet A. T., no. 3.

- —
i; a:
«
- a
— : .
is - 2789
‘- ~

2783

2784

2785

2786
2787

2788

2794

9795 )

‘Guts on ¢
branch of sc
Genesee. 1700 feet J ae ae

North side of hill between Coon hollow a pe
Genesee township; ear in read."
no. 9. tise tae

Woodchuck rin 4 mile from intersactiaafll
Hinsdale road. 1460, 1500, 1505 feet A. 1, 1 10. 12.

Near mouth of Gull brook about 1 mile west of Hin:
also loose in forks of road west of Gull brook. eS 3
1510, 1520 feet A. T., no. 12; [H 137] 1970 fee 3
(loose), no. ? ri De

Head of Fay hollow, Hinsdale. 1950 feet A. Tn no. 9 se

Near summit of Fay hollow about 1 mile north of Penn nsy wt
vania R. R. 1525 and 1585 feet A. T., no. 12. | a “a

Ravine 50 yards north of Erie depot, Hinsdale, east of r ile
road track. 1500 feet A. T., no, 12. “ae

Bank of creek in eastern part of Hinsdale towndiin aaa
county line, about 35 miles northeast of Haskell eas
1690 feet A. T., no. 11. -

Ravine 4 mile northwest of Haskell Flats, } mile west of
junction of roads. 1680 feet A. T., no. 11. i:

Cut by roadside, road from Scotts Corners eastward to.
Haskell Flats, Hinsdale township. 1840 feet A. T., no. 9. —

Old quarry on hillside just west of Haskell Flats. 1695
feet A. T., no. 10. a

Roadside ditch on spur of 2185 feet summit, 3 miles south-_
west of Cuba. 2045 feet A. T., no. 9. E

Top of hill about 2 miles southwest of Cuba. 2045 feet —
A. T., no. 9. a

2170 feet summit west of Oil creek, half way between —
Cuba and Hinsdale. 2170 feet A. T., no. 9. ;

2805

2806

2807

2808

REPORT OF THE STATE PALEONTOLOGIST 1901 495

Ravine on west side of Oil creek valley about 3 miles
northeast of Hinsdale. 1585 feet A. T., no. 12.

Road north and south over 2150 feet summit just south
of Hinsdale-Ischua boundary, 14 miles east of north-
western corner of Hinsdale township. 2100 feet A. T.,
no. 9.

Mouth of ravine entering Oil creek on valley from north-
west, 3 miles west of Cuba. 1540 feet A. T., no. 12.

Summit of Dutch hill, Hinsdale township. 2235, 2220 feet
A. T. (loose). |

Mouth of ravine entering Ischua valley from northeast
2 of a mile north of Scotts Corners. 1555 feet A. T.,
no. 12.

Roadside 1 mile due north of Humphrey Center. [Hu

206] 1920 feet A. T., no. 8?; [Hu 2061] 1845 feet A. T.

(loose), no. 9?

Horizon?

Hill road from Humphrey Center to Cooper’s hill; west
side. [Hu 207] 1770 feet A. T., no. 9? [Hu 207+] 1930
feet A. T., no. 9.

Roadside top of Cooper’s hill, northwestern part of Hum-

2225 feet A. T., no. 8?

From head, down to near mouth of ravine entering val-

phrey township; loose.

ley of Five Mile creek from north, just west of Ischua-
Humphrey boundary. [Hu 210] 1945 feet A. T.; [Hu
2107] 1870 feet A. T.; [Hu 210*] 1850 feet A. T., no. 10;
[Hu 2104] 1790 feet A. T.; [Hu 210°] 1760 feet A. T., no.
at.

Northern end of Ischua township about 2 miles west of
south end of Cuba reservoir; also loose top of 2217 feet
summit slightly southwest of reservoir. [I 178] 2080,
2130 feet A. T., no. 9; [1179] 2210 feet A. T., no. 9.

Ravine intersecting Oil creek valley from northwest 2

1670 feet A. T., no. 12.

Outcrop by stream 1 mile due east of Ischua depot, south
side of valley. 1615 feet A. T., no. 12.

Road running east from Ischua; about 1 mile east of
Ischua. 1718, 1800 feet A. T., no. 11.

miles west of Cuba.

ao) ay, 2 '
a a ee

Be Sts “ae
# cr Ravine entering thay rm st :
Ischua; } mile up ravine ete main 1
AL), n0: 12 ¥ 7 a
2813 Deep gorge running north rare road 3 willestil
Ischua; 50 yards up gorge. 1860 feet A. 7, no
2814 Near 2015 feet summit, 1 mile north of Hinsda
boundary, in Ischua township. 2000 feet A. oe }
2815 Near road 4 miles south of Ischua. 1810 feet A. se a : ot
2816 Roadside 44 miles south of Ischua. 2040 feet A. Tm D
2817 Top of Learn hill, northern part of Ischua toy

ta

2160-2280 feet A. T. (loose), no. 7 or 8. i ‘ee
ee
2818 East bank of Ischua creek, + mile south of Ischua. sited
feet A. T., no. 13. | y eae

2819 Road running near middle of Lyndon cowie + mile
north of Lyndon-Ischua boundary. 2080 feet A. T.,
no. 9. Bs,

2820 Southwest corner of Lyndon township, just southeste of
four corners 4 mile east of Lyndon-Franklinville bound- —
ary and 14 miles north of Lyndon-Ischua von
2140 feet A. T., no. 11.

2821 Quarry below reservoir about 1 mile south of Olean. |
1560 feet A. T., no. 11.

2822 Near brow of steep escarpment facing north; 1} miles —
south of Olean. 1745, 1750, 1760, 1765, 1890, 1900 feet _

A. T., no. 9. “4
2823 Old quarry on north slope of Mount Hermon. 1970 feet
A. T,, 20.'%

2894 Old quarry on west side of Mount Hermon, about 44 miles
south of Olean. 2040 feet A. T., no. 7.

2 &B ket on northeast side of hill 24 miles Saamen? of
fe ee. ‘Olean. eee tek, A Tne. 7

ci. & Bradford trolley road. 2200, 2275, 2300 feet

eke: 7A. T., no. 3.

98 32 Top of high hill with masses of conglomerate, 34 miles

. . slightly southwest of Olean. 2300 feet A. T., no. 3.

@ 2833 Quarry in Mount Hermon sandstone, Two Mile valley, 4

Bo: miles southwest of Olean. 2090 feet A. T., no. 11.

f 2834 Cut on old narrow gage railroad from 3-5 miles southwest

| of Olean; also loose on bank of excavation. 1920-50

Meee! ‘fect A, 'T., no..7. - |

_ 2835 34 miles southwest of Olean. 2125 feet A. T., no. 5.

2836 Cut on abandoned narrow gage railroad between Two

Mile and Four Mile valleys, 24 miles northeast of Rock

City. 2160, 2170 feet A. T., no. 4.

2837 Old quarry east of road, and on north side of hill on road
from Wayman branch to Olean about 1 or 2 miles south-
east of Olean. 1650, 1775, 1875, 1900 feet A. T., no. 9.

2838 Quarry on road from Wayman branch to Olean, 1-3 miles
southwest of Olean. 2050 feet A. T., no. 8.

2839 Woods at east of 2240 feet hill, 4 mile south of Wayman
branch, 4 or 5 miles southeast of Olean. 1750 feet

ad ee ee
2840 Near top of 2240 feet summit, southeast corner of Olean
township. 2175 feet A. T., no. 3.

2853

2854

2855

2856

2857

2858

Loose; top of bench on north side of 2224 tiie hill 1 ae .

_—
De a

Mouth of ravine oe mile
feet A. T., no. 11. - a, n
On Western N. Y. “& Pa. BR, (Bradford a
southwest of Olean. 1750, 1850 feet A. 7, er
Cut on Pennsylvania R. R. near United pipe line pt |
station, Olean. 1450 feet A. T., no. 12. | * ;
Near mouth of Louds creek near New York-Penn ex yan
boundary. 1480 feet A. T. (loose), no. 8?
Outcrops at spring by roadside 245 miles northwe
Olean. 1640 feet A. T., no. 10. a
Old quarry on hillside west of Olean-Hinsdale anh :
south of Woodchuck hollow. 1670 feet A. T., no. 10,
Old quarry on second road west from Olean. 1670 f c i S.
A. T., no. 10. eae
Quarry } mile northwest of Erie depot, Olean. 1650 tect
A. T., no. 10. ; i
Bank of Dodges creek just above bridge on northeastern
outskirts of Portville. 1445, 1480 feet A. T., no. 11.

of oil r 1er
anal ag —— oe

a H

west of Portville. 2050 feet A. T., no. 3.

West side of Wolf run opposite 2378 foot summit.
[P 72] 1620 feet A. T., No. 11.

North bank of Haskell creek about 3 miles northeast of
Boardman. 1600 feet A. T., no. 11.

Roadside cut on summit between Boardman and Haskell
creek. 1750 feet A. T., no, 9

South bank of Allegany river at Weston Mills, opposite
Riverhurst park. 1420 feet A. T., no. 11.

Just west of Haskell creek, opposite junction of Wolf
run. 1550 feet A. T., no. 11.

2869

2870

2871

REPORT OF THE STATE PALEONTOLOGIST 1901 499

Outcrop in field by road to Wayman branch 3 mile south-
west of bridge at Portville. 1500 feet A. T., no. 11.

Loose; south of first summit of ridge south of bridge
across the Allegany river at Portville. No. 7.

Cut on Pennsylvania R. R. near bridge over Oswayo creek
4 mile south of Portville. 1485 feet A. T., no. 11.

Loose in field north of Carrollton. 1470 feet A. T., no. 8.

Road on south bank of Allegany river in southwest out-
skirts of Portville. 1450 feet A. T. (loose), no. 11?

Near head of west branch of Gull brook, 3 miles south-
west of Ischua. 1890 feet A. T., no. 11.

Loose; south spur of 2100 feet hill about 24 miles north-
west of Allegany. 1910, 1960 feet A. T., no. 7.

Quarry on east side of Cuba reservoir near dam. 1595
feet A. T., no. 13.

Roadside, bank of Indian creek, Eldred, McKean co. Pa.
3-4 miles south of state line. i540 feet A. T., no. 9.
Roadcut 100 rods north of Bowler station on Central
New York and Western R. R. Genesee township. 1560,

1600 feet A. T., no. 11.

From block of hard sandstone firmly embedded in road
and ditch, 2 miles south of Little Genesee. 1850 feet
Az 'T., no. 9?

Road on top of hill 1 mile east of Hinsdale. 1980 feet
me nO: “9.

Road ditch on boundary between Ischua and Hinsdale in
northwestern corner of northern jog of Hinsdale. 2020
feet A. T., no. 9. )

Ravine on west side of valley 4 mile south of Cuba. 1600
feetea. I. NO. 12,

Roadcut at northeast of Dutch hill in northwestern cor-
ner of Hinsdale township. 1810 feet A. T., no. 10.

Outcrop of sandstone 4 mile northeast of Ischua depot

near road forking. 1610 feet A. T., no. 12.

Locality numbers 2875-2900 and 3057-3094 represent fossils
collected by Charles Butts during 1901 in area covered by the

2875

2876

2883
2884

2885
2886

=e ‘Shales an ;
6 Wolf as Hage cal gi ve |
7 Shales and sandstones - bt
8 Shales and sandstones. | Orthothe
9 Cuba sandstone . ye

At angle in road after passing north over hill at
Newton run, 3} miles north of Salamanc Ce . 8 tat
313, no. 5.

North side of road from Little Valley ‘creek é Sllicot
ville near top of hill, } mile as cag of E es ‘
Station 314, no. 7. oe :

Riverside drive 1 mile south of Ellicottville. |
no. 8.

West side of Great Valley creek, about 14 miles southwe
of Great Valley. Station 316, no. 8.

Face of steep bluff west of Great Valley creek, 14 m
southwest of Great Valley. Station 317 and 317}, no. 7. |

Head of Mutton hollow just north of northern boundary rf.
of Salamanca sheet. Station 318, no. 4. . ae

Cut on Buffalo, Rochester and Pittsburg railroad at out
21 miles north of Great Valley. Station 319, no. 7. — * :

Road about $ mile northeast of Killbuck station. Station
320, no. 7. i k

Old road over north side of hice 2-3 miles northeast of |
Killbuck. Station 321, no. 1 5

Head of hollow about 1 mile ae of Peth. Station 322,
no. 7.

Near mouth of Barker run. Station 323, no. 8.

Collected west of head of Barker run. Station 324, no. ?—

It

- REPORT OF THE STATE PALEONTOLOGIST 1901 501

Near 2180’ summit, slightly southeast of Sugartown.
Stations 325, 3251, no. 7.

Road west of Five Mile creek and 2-3 miles southwest of
Cooper hill. Stations 327, 3271, no. 7.

Road about ? mile south of summit of Cooper hill. Sta-
tion 328, no. 7.

One mile south of Cooper hill and $ mile west of county
line, Humphrey township. Station 329, 3291, no. 7.
Road ditch on Wrights creek road near head, about ? mile

northwest of Bozard hill. Station 330, no. 7.
2892 Road about # mile northwest of Humphrey Center. Sta-
. tion 331, no. 7.
2893 Road short distance north of crest of ridge at head of
Nine Mile creek. Station 332, no. 7 (loose).
2894 State line on Olean, Rock City and Bradford trolley road.
Station 333, 33314, no. 2.
2895 Inroad near head of Limestone brook. Station 334, no. 3;
station 3341 2, no. 4.
2896 Limestone brook, 2-3 miles west of Limestone. Station
ay TIO. C.
2897 Near head of southwest branch of Limestone brook. Sta-
tion 336, no. 3.
2898 Summit of high hill just north of state line and near
boundary between Salamanca and Carrollton town-
ships. Station 387, no. 2.
2899 Near head of east branch of Bolivar creek, Bradford co.
Pa. Station 338, no. 2; station 3387, no. 1.
2900 Trolley cut 4} mile west of Knapp Creek. Station 339,
no. 2. 20-30 feet below summit at Knapp Creek on
road to Four Mile. Station 3391, no. 3
For continuation of localities in Salamanca quadrangle area
see record numbers 3057-3093.
The following localities from 2901-48 represent material from
the collection donated by J. M. Clarke, 1901. On the tickets
each of these numbers is preceded by the letter C.

2905

2906

2907

oe *” BM GE: oe

co. J. M. Clarke, donor. 1901. —

Genesee shale (Styliola a ays ne)
J. M. Clarke, donor. 1901. ;
Genesee shale. Bristol Center, Ontario « co. JI.M
donor. 1901. m4 =
Genesee shale. Livingston co. J. M. Clarke, d it) mor.
Genesee shale; base of shales. Bell’s gully, Car n andai
lake. J. M. Clarke, donor. 1901. ae
Naples beds. Various outcrops in- the Naples 3 vi alle ley
J. M. Clarke, donor. 1901: seit =

~~

Naples beds; goniatite layer. Parrish gully, a

tario co. J. M. Clarke, donor. 1901. oa pen
Naples beds. Mount Morris, Livingston co. J. M. Cl:
donor. 1901.
Naples beds. Cashaqua creek. J. M. Clarke, donor i
Naples beds. Honeoye lake; mostly young goniatit
J. M. Clarke, donor.. 1901. Le
Naples beds. Conesus lake. J. M. Clarke, donor. 1901. %
Naples beds. Rock stream, Yates co. J. M. Clarke, donor. — y
1901. 7
Chemung beds. Elmira. Goniatites. J. M. Clarke, donor. —
1901. a
Middle Devonic (Goniatitenkalk). Bredelar, Westphalia. — ;
J. M. Clarke, donor. 1901. 4
Onondaga limestone. Canandaigua town. J. M. Clarke,
donor. 1901.
Helderbergian. Albany co. J. M. Clarke, donor. 1901.
Naples beds; sandstone slabs from upper layers with —
goniatites. Naples valley. J. M. Clarke, donor. 1901.

.
+

—
ds; v ani eck band. Sparta town. Cut on-

. Le & w. R. R. 6 miles northwest of Dansville,

vgston co. Fish remains. J. M. yoren: donor. —

24 Wiscoy beds. Castile, Wyoming co. J. M. Clarke, donor.
1901. 3 : |

- Genesee shales; bituminous band. Woodville, Ontario

eo. J. M. Clarke, donor. 1901.

6 Genesee shales. Various localities on Canandaigua lake.

sd. M. Clarke, donor. 1901.

2907 Genesee shales. Gull berg, Honeoye lake. J. M. Clarke,

4 Ze donor. 1901. eae .

2928 Genesee shales; upper layers. Yates co. J. M. Clarke,

a donor. 1901.

_ 2929 Genesee shale (Styliola limestone), Bristol Center, On-

er | tario co. J. M. Clarke, donor. 1901.

2930 ‘Naples beds. Hamilton gully, Honeoye lake. J. M.

a Clarke, donor. 1901.

_ 2931 Chemung beds. Alfred, Allegany co. J. M. Clarke,

: donor. 1901.

_ 2932 Chemung beds. Avoca, Steuben co. J. M. Clarke, donor.

a 1901.

a 2933 Chemung beds; lower. Prattsburg, Steuben co. J. M.

Clarke, donor. 1901.

2934 Outlier of Ithaca beds; third falls of Grimes gully,
Naples, Ontario co. J. M. Clarke, donor. 1901.

2935 Chemung beds. Base of High point, Naples. J. M.
Clarke, donor. 1901.

2936 Marcellus shales with spores. Canandaigua. J. M.

“Clarke, donor. 1901.

2937 Chemung beds. Near Wellsville, Allegany co. J. M.
Clarke, donor. 1901.

=_

Clarke, donor. 1 Se a
Naples beds. Pontiac, Erie, co. rs Pins
Naples beds. Fox's point, Lake Erie. J : M.C la mi
1901. | ae
Naples beds, loose blocks containing ithaca
Canandaigua lake. J. M. Clarke, donor. 190 =
Marcellus shale. Slate rock falls 4 miles south
Geneva, Ontario co. J. M. Clarke, donor. rt z
Chemung beds. Canandaigua. J. M. Clarke, donor. 19( 1. ¥
Utica slate. Dolgeville, Herkimer co. J. M. 7 ee
donor. 1901. | Bac Ps
Helderbergian. Orange co. J. M. Clarke, donor. “190 )1
Helderbergian. Cumberland Md. Ward & Howell a
chase. 1901. ‘
Rondout waterlimes. Loose at Canandaigua. J. Me i
Clarke, collector. 1901. ae ar
Hamilton shales. Robertson’s quarry, Canandaigua.
J. M. Clarke, collector. 1901. =
Salina beds. Black shales below green shales. Bottom 5
of Erie canal, 14 miles northwest of Pittsford, Monroe a
co. J. M. Clarke, collector. 1901. |
Guelph dolomite. Elora Ont. J. M. Clarke, collector.
1901.
Marcellus shales. Canandaigua. J. M. Clarke, collector.
1901. §
Ithaca beds. North glen at McKinney’s, Cayuga lake. — |
100 yards above falls. C. A. Hartnagel and H. 8. Mat-
timore, collectors. 1901.

og

2959

2960

2961

2962

2963

2964

2965

2966

REPORT OF THE STATE PALEONTOLOGIST 1901 505.

Ithaca beds. South glen at McKinney’s, Cayuga lake.
100 yards above high falls. C. A. Hartnagel and H. S.
Mattimore, collectors. 1901.

Lower Portage beds. 4 mile below Esty glen, Tompkins
co. along railroad track. At this place the Genesee
is about 12 feet above the lake and contact between
Genesee and Portage is well shown, the former capped
by a hard blue sandstone 24 feet thick. C. A. Hart-
nagel and H. 8S. Mattimore collectors. 1901.

Lower portage beds. Asbury, below Bower’s mill falls,
+ mile east of Portland. 980 feet A. T. C. A. Hart-
nagel and H. S. Mattimore, collectors. 1901.

Lower Portage beds. Asbury, 100 yards below Bower’s
mill falls, 4 mile east of Portland. 975 feet A.T. ©. A.
Hartnagel and H. 8. Mattimore, collectors. 1901.

Ithaca beds. South glen at McKinney’s, Cayuga lake.
150 yards above high falls.. C. A. Hartnagel and H. S.
Mattimore, collectors. 1901.

Ithaca beds. Right branch of Salmon creek, 3 miles
north-northeast of Ludlowville. 540 feet A. T. C. A.
Hartnagel and H. S. Mattimore, collectors. 1901.

Lower Portage beds. First branch of Salmon creek, 1
mile northwest of Ludlowville. 780 feet A. T. C. A.
Hartnagel and H. 8S. Mattimore, collectors. 1901.

Lower Ithaca beds. Creek bed just east of highway, 13
miles east of Portland, Cayuga lake. C. A. Hartnagel
and H. S. Mattimore, collectors. 1901.

Ithaca beds. North glen at McKinney’s, slightly higher
than 2563. C. A. Hartnagel and H. 8. Mattimore, col-
lectors. 1901.

Ithaca beds. South glen at McKinney’s, Cayuga lake,
above 2564. C. A. Hartnagel and H. S. Mattimore, col-
fectors:. - 1901.

Ithaca beds. South glen at McKinney’s, Cayuga lake, 50
yards from point where creek divides. C. A. Hartnagel
and H. S. Mattimore, collectors. 1901.

2969

2970

2971

2972

2973

2974

2976

2977

from whose wells th — r
Portage 0 teat |

Genesee | 125, Re,
Tully | ed
Hamilton 1079? “
Marcellus le ear

2137 feet to first salt; total depth 2190 feet. a best

Ithaca beds. Renwick creek; short distance abe ) ae
C. A. Hartnagel and H. 8. Mattimore, collector 7 BS 7

Ithaca beds. Renwick creek, just above 2969.
Hartnagel and H. 8. Mattimore, collectors. 1901.

Ithaca beds. Foot of Ithaca falls, Fall creek, | Itha
C. A. Hartnagel and H. 8. Mattimore, collectors. 1901. —

Ithaca beds. Top of Ithaca falls, Fall creek, Ithaca. o =
Hartnagel and H. 8. Mattimore, collectors. 1901. on

Ithaca beds. Creek bed foot of cascade at electric light —
plant, Fall creek, Ithaca. C. A. Hartnagel and H. 8S. —
Mattimore, collectors. 1901. 2

Ithaca beds. Creek bed just above electric light pia a
Fall creek, Ithaca. C. A. Hartnagel and H. 8S. Matti-
more, collectors. 1901.

Ithaca beds. Foot of first falls above electric light plant,
Fall creek, Ithaca. C. A. Hartnagel and H. 8. Matti-
more, collectors. 1901.

Ithaca beds. Top of falls above 2975. C. A. Hartnagel
and H. 8. Mattimore, collectors. 1901. |

Oneonta beds. Camp Heart’s Content, below falls, Law-
rence station, Greene co. G. H. Chadwick, collector.
1901.

Le

bes

2980

2981

2982

2983

2984
2985
2986
2987

2988

REPORT OF THE STATE PALEONTOLOGIST 1901 507

Ithaca beds. Creek bed at Weaver’s falls 1 mile north-

west of Groton, Tompkins co. C. A. Hartnagel and
H.S. Mattimore, collectors. 1991.

Ithaca beds. 100 yards above 2978. C. A. Hartnagel and
H. S. Mattimore, collectors. 1901.

Ithaca beds. Ben Hatch farm 24 miles north of Groton.
C. A. Hartnagel and H. 8. Mattimore, collectors. 1901.

Ithaca beds. Hollow brook, Locke, Cayuga co. This
station is 2 miles southwest of Locke above Genesee
shale, which is exposed in lower portion of brook.
C. A. Hartnagel and H. 8. Mattimore, collectors. 1901.

Beekmantown limestone. Graptolites. Abandoned
quarry 1 mile southeast of Melrose and 4 mile east of
Grant Hollow, Rensselaer co. R. Ruedemann and H. 8.
Mattimore, collectors. 1901.

Guelph dolomite. Balantine’s quarry east of river, south
of railroad station, Galt Ont. Lowest part of Galt
section; according to Logan about middle of formation.
J. M. Clarke and D. D. Luther, collectors. 1901.

Guelph dolomite. Hogg’s quarry west of river; Galt
Ont. About same horizon as 2983. J. M. Clarke and
D, D. Luther, collectors. 1901.

Guelph dolomite. Mill dam at Galt Ont. Horizon just
above 2984. J. M. Clarke and D. D. Luther, collectors.
1901.

Guelph dolomite. Melross’s quarry east of river, 1 mile
moren Of Galt Ont. Top of Galt section. J. M.
Clarke and D. D. Luther, collectors. 1901.

Guelph dolomite. Hespeler Ont. According to Logan
near base of section. J. M. Clarke and D. D. Luther,
collectors. 1901.

Guelph dolomite. Webster’s quarry, Galt Ont. J. M.
Clarke and D. D. Luther, collectors. 1901.

2989a-r- Cox’s ravine, Cherry Valley, Otsego co.

a Marcellus shale in Cox’s ravine below falls
b Marcellus shale directly below Anarcestes bed hori-
zon about 10 feet

2990

2991

2992

2993

2994

2995

2996

2997

2998

2999

o Intercalated abate ah Steenburg fa
p Limestone bed 7 (base on stenbaen
q Limestone bed; middle part

r Limestone bed; upper part

R. Ruedemann, collector. 1901.
Agoniatites limestone. Lamoreaux farm, 1 nites
Schoharie. R. Ruedemann, collector. 1901. 7 i: 5
Marcellus shale. Stony point, ‘West Seneca, Erie

B. F. Morgan, collector. 1901. < ms i
Chemung beds. Near Union, Broome co. J. Vaal Deloo, » iF |

collector. 1901. ee
Chemung beds. Kirkwood, Broome co. E. B. Hall, donor.

1901. be:
Chemung beds. Near Tracy Creek, Broome Co. E. am
Hall, donor. 1901. rs
Chemung beds. Ouaquaga, Broome co. E. B. Hall, i
donor. 1901. =,
Guelph horizon. On canal feeder 24 miles south of Shelby,

Orleans co. D.D. Luther, collector. 1901.

Chazy beds. Roadside 300 feet west of D. & H. BR. B.
track at Valeour station, Clinton co. G. van Ingen,
collector. 1901.

Chazy beds. Ledges in fields to north of normal school,
Plattsburg, Clinton co. G. van Ingen, collector. 1901.

Beekmantown limestone. Along D. & H. R. R. tracks in
eut near Burdick’s crossing, 14 miles north of Crown
Point, Essex co. G. yan Ingen, collector. 1901.

3003

3004

3005

3006

3007

3008

3009

3010

REPORT OF THE STATE PALEONTOLOGIST 1901 509

Potsdam sandstone. Bed of Saranac river near “ Mill D”
at Kent Falls, 74 miles west of Plattsburg, Clinton co.
G. van Ingen, collector. 1901. ,

Potsdam sandstone. Same locality as 3000, but 60 feet
higher and 400-+ feet farther down the river. G. van
Ingen, collector. 1901.

Potsdam sandstone. In bank of Saranac river above
“Mill D” at Kent Falls. Horizon is immediately
below that of 3001 and 53 feet above that of 3060.
G. van Ingen, collector. 1901.

Chazy limestone. Bed of Saranac river just below the
“Main mill dam” about 2 miles west of Plattsburg.
G. van Ingen, collector. 1901.

Potsdam sandstone in bed of Little Ausable river at
Schuyler Falls, Clinton co. G. van Ingen, collector.
1901.

Chazy limestone at east side of West Chazy to Chazy road,
14 miles northeast of West Chazy station, Clinton co.
G. van Ingen, collector. 1901.

Potsdam-Beekmantown transition beds on road from
Champlain to Chazy, west road (westerly of the two
south bound roads), at top of hill about 2 miles south of
Champlain, Clinton co. G. van Ingen, collector. 1901.

Potsdam sandstone at bridge over Carbeau creek at three
corners, # mile west of Coopersville, Clinton co. G. van
Ingen, collector. 1901.

Potsdam sandstone in fields on Champlain to Chazy east
road about # mile north of the four corners west of
Cooperville, Clinton co. G. van Ingen, collector. 1901.

Potsdam-Beekmantown transition beds on Champlain to
Chazy east road, 2 miles south of Champlain. G. van
Ingen, collector. 1901.

Potsdam-Beekmantown transition beds on Champlain to

; Chazy east road, 2 miles south of Champlain. Horizon
4 feet above that of 3009. G. van Ingen, collector.
1901.

3014

3015

3016

3017

3018

3019

3020

3021

mile above pliowen. of Marble and Sha ates Iga;
miles north of Chateaugay, Franklin co. G.ya nin
collector. 1901. come:

Potsdam sandstone in Marble river near Pat.
mile north of Chateaugay, Franklin co. Gora ye un
collector. 1901. | ee

Potsdam- Beclanapions transition beds in bewii ot

2
«
t

village of Ticonderoga, Essex co. G. van "Ingen, s
lector. 1901. ; ce %

Potsdam-Beekmantown transition beds tebe ‘whore: a
Lake Champlain on west side of Mt Independence near —
A. A. Blood’s house, in town of Orwell, Addison co. iS
G. van Ingen, collector. 1901. | ate

Beekmantown beds in bed of Boquet river in village o
Willsboro, Essex co. G. van Ingen, collector. 1901.

Beekmantown beds on shore of Lake Champlain at Mate “
child’s point at mouth of Boquet river, town of Wills-
boro, Essex co. G. van Ingen, collector. 1901.

Potsdam sandstone on lake shore at Flat Rock point, 2
miles east of Willsboro, Essex co. G. van Ingen, col-
lector. 1901.

Beekmantown beds. Bed of Salmon river at crossing of
Salmon river road at South Plattsburg. G. van Ingen,
collector. 1901.

Mytilus edulis bed in raised beach at the “ Gravel
pit” 1 mile west of Lapham Mills, Clinton co. G. van
Ingen, collector. 1901.

|
8026
;
|
E - 3027

3028
3029

3030
3031

3032

3025

REPORT OF THE STATE PALEONTOLOGIST 1901 511

Potsdam sandstone in bank of Saranac river at lower end

of “ Mill D” at Kent Falls, 73 miles west of Plattsburg.
Horizon 258 feet above that of 3000. G. van Ingen, col-
lector. 1901.

Potsdam sandstone in bank of Saranac river at lower end
of “ Mill D” Kent Falls. Horizon immediately above
that of 3022. |

Chazy limestone. Road from West Chazy to Chazy, 14
miles east of West Chazy, Clinton co. G. van Ingen,
collector. 1901.

Potsdam-Beekmantown transition beds in bed of Big

_ Chazy river at the Champlain waterworks and dam, 14
miles west of Champlain, Clinton co. G. van Ingen, col-
lector. 1901.

Potsdam sandstone. On Champlain to Mooers road, 2%

. miles east of Mooers, Clinton co. G. van Ingen, col-
lector. 1901.

Potsdam-Beekmantown transition beds in village of Ticon-
deroga, near the junction of East Exchange and River
streets. G. van Ingen, collector. 1901.

Potsdam-Beekmantown transition beds near the junction
of East Exchange and River streets in the village of
Ticonderoga. 10 feet above 3027. G. van Ingen, col-
lector. 1901.

Potsdam-Beekmantown transition beds on left bank of
Ticonderoga creek at north side of mill, below East
Exchange street bridge, Ticonderoga. G. van Ingen,
collector. 1901.

Trenton shales in bed of Saranac river at South Catherine
street bridge in village of Plattsburg. G. van Ingen,
collector. 1901.

Potsdam sandstone. Ausable chasm at the place called
“Mecca”, just below the “Devil’s Oven”. Ausable
chasm, Clinton co. G. van Ingen, collector. 1901.

Potsdam sandstone. Same layer as 3031 but exposed at
the mouth of Mystic gorge in Ausable chasm, about 200
feet down stream from 3031. G. van Ingen, collector.
1901.

3036

3037

3038

3039

3040

3041

3042

down aia 3082. A chas
- Ingen, collector. ne Kae as
Potsdam sandstone. - Same mine as 3 131 dye but te
level of path-railing at the “ Postofiice ”, 2 50 f
stream from 3034. Ausable ours a van
collector. 1901.
Potsdam sandstone. Same layer as 3031, bat e > te se
hillside at upper rapids below Cathedral - er
point about 2100 feet down stream from 3005. sak
chasm. G. van Ingen, collector. 1901. — 2 ; a

Potsdam seeped ui Same lags as 3031, ree

1901. "toa “st
Potsdam sandstone. Layer just below 3033 at level ¢ of
path-railing between “Mystie gorge” and « Smu g-
gler’s pass”, Ausable chasm. G. van Ingen, collector.
1901.
Potsdam sandstone. Hyolithes bed at level of + Table
rock” at foot of Cathedral Rocks, Ausable chasm. an ;

le
.

™

.

yan Ingen, collector. 1901. ‘3
Potsdam sandstone. Same layer as 3039, but exposed in
hillside at Upper Rapids below Cathedral Rocks,
Ausable chasm. G. van Ingen, collector. 1901.
Potsdam sandstone. Obollela layer, 15 feet above 3036 —
in hillside at Upper Rapids below Cathedral Rocks,
Ausable chasm. G. van Ingen, collector. 1901.
Potsdam sandstone. Obolella layer at top of Cathedral — "4
Rocks, 50 feet above 3036, Ausable chasm. G. van
Ingen, collector. 1901. |

=:

-
"ys

3052

3056

REPORT OF THE STATE PALEONTOLOGIST 1901 513

Chazy limestone. Drift on shore of Lake Champlain at
Port Kent. G. van Ingen, collector. 1901.

Beekmantown beds. In field west of D. & H. R. R. track
and north of wagon road that crosses the railroad 1
mile north of Beekmantown station, Clinton co. (Whit-
field’s locality of Ophileta beds. Am. mus. nat. hist. 2)
G. van Ingen, collector. 1901.

Potsdam sandstone. “Layer with Linguloid shells 15 feet

- above 3039 at foot of stairs leading up cliff at Cathe-
dral Rocks in Ausable chasm. G. van Ingen, collector.
1901.

Chemung beds. West hill, Lincoin gully, Naples. 1380
teen A TD. D: Luther, collector... 1901,

Lockport (?) dolomite. Pittsford; on Allen creek 4 mile
west of canal. D.D. Luther, collector. 1901.

Guelph dolomite. Galt, Ont. William Herriot, donor.
1902.

Chemung beds. Hamlin pasture 2 miles southeast of
Naples on Knapp hill. D. D. Luther, collector. 1901.

Chemung or Ithaca beds. West hill above Cumming’s
crossing, Naples. D. D. Luther, collector. 1901.

Lockport (?) dolomite. Pittsford; on Allen creek be-
tween canal and Auburn R.R. D. D. Luther, collector.
1901.

Salina beds. Black shale lying at or near the base of
the Salina formation. Pittsford; canal bank near Cold
Spring House. D. D. Luther, collector. 1901.

Chazy limestone. Day point, Valcour. G. van Ingen,
collector. 1901.

Portage (Ithaca) shales. Spafford, Onondaga co. D. D.
Luther, collector. 1895.

Naples shales. Plum creek, village of Himrod, Yates co.
170 feet above Seneca lake. J. M. Clarke, collector.
1895.

Naples shales. Belknap’s gully 2 miles north of Branch-
port, Yates co. J. M. Clarke, collector. 1895.

Continuation of record of localities of fossils collected in area

covered by Salamanca-quadrangle. Charles Butts, collector.

1901.

See section, 2875.

side ent of oncom of Bova and
Station 266, no. 7. od
Hillside east of junction of Bova aia ‘Rea H
40 feet above station 266. Station 267, no. ’ ; "
Crest of nose east of junction of Bova and I
creeks. Station 268, no. 7.
Buffalo, Rochester and Pittsburg railroad cut 2
way crossing at Carrollton. Station ies no. 8 1
Old quarry just above highway, short dist $0 aa of f
Carrollton. Station 272, no. 7. a “ah , ea
ae of nose nearly 1 mile due east of Carrollton. | St tio a :
273, no. 7. }
Crest of nose east of Carrollton. Station 275, no. 3. ae =
15 feet of top of 2200’ summit east of Carrollto
Station 276, no. 3. = *
Roadside head of hollow, little over 1 mile southeast of |
Sugartown, Humphrey township, near western boun- -

a

ve a, a.

dary. Station 326, no. 7.
West side of hill between Chipmunk and Tuna per ee
Station 278, no. 7; station 277, no. 7. a
Crest of ridge between Chipmunk and Tuna creeks, nearly
due east of Irvine Mills. Station 280, no. 4. a
Near forking of Irish and Rice brooks, west of Tuna
creek. Station 281, no. 7. ">
Roadside a few rods west of road forking Irish brook
and Rice brook roads. From boulder. Station 282, -
no. 4.

ist mae of summit by road, 3 miles noth of Sala-
manca, at head of Newton run. Station 312, no. 3.
Road near McIntosh creek 14 miles from Red House —
; brook. Station 289, no. 7. z ra Seago PD)
) Crest of ridge between Tuna and pens creeks.
Station 291, no. 4. : |
North slope of ridge between Tuna and Chipmunk creeks.
| Station 292, no. Lae 2
North slope of ridge between Tuna and Chipmunk creeks,
30 feet below station 292. Station 293, no. 7.
1 mile east of Riverside junction, Carrollton township,
50 feet below station 294. Station 295, no. 7.
3083 1 mile east of Riverside junction, Carrollton township,
of 50 feet below station 295. Station 296, no. 7.
3084 Roadside just south of junction of roads at twine mills,
Tuna Valley. Station 297, no. 7.
3085 Hill north side of Killbuck station. Stations 298-800,
a no. 7.
3086 Hill south of Salamanca. Station 302, no. 7; station
fen ele“, no, (; station 302°) 4 no. 4.
3087 Cut on Buffalo, Rochester and Pittsburg railroad, 2 miles
- east of Salamanca. Station 303, no. 7.
8088 Cut on Buffalo, Rochester and Pittsburg railroad, 3-4
miles east of Salamanca. Station 304, no. 8.
3089 Spur west of Carrollton and west of river. Station 305,
BOD ft. 3
3090 Roadside on road northwestward up Great Valley creek,
~ about #2 mile north of Killbuck station. Station 306',
nO. 1.
3091 Road, Hungry hollow, 3 miles west of Great Valley.
Station 307? 2, no. 7.

burg, donor.
107 Upper Siluric. Island of ee

chased of Dr F. Krantz (Mfineralien-Cont
many. 1901.

Pad

i tee th da

APPENDIX 3

_ CONTACT LINES OF UPPER SILURIC FORMATIONS ON

THE BROCKPORT AND MEDINA QUADRANGLES
TRAVERSES BY J. M. CLARKB, R. RUEDEMANN AND D. D. LUTHER, 1901

Brockport quadrangle. Clinton beds. At Adams Basin on the

_ Niagara Fails road the Clinton limestones are exposed at one

or two points along the banks of Salmon creek. Not far back
from the railroad culvert crossing this creek was formerly a
small quarry in the cherty thin limestone slabs of the upper
Clinton (station 18; 520+feet A. T.).

Station 15. In the bottom of Salmon creek at crossing of
first east and west road south of Adams Basin, thin relatively
pure Clinton limestones with Hyattella congesta

- (elevation 525 feet A. T.).

Still farther up stream and along the east branch about 4
mile are more silicious Clinton flags lying close to the top of the
series. |

Rochester shale. Station 17; 20 rods beyond this point on the
same stream is an outcrop of Rochester shale with Spirifer
radiatus, Dalmanites limulurus, ete. This is
the base of the Rochester shale and its elevation is 570 feet
A.T. The change from the Clinton to the Niagara shale is not
marked by topographic features and there appears to be no sur-
face evidence of the passage of the one formation into the other.
South of Spencerport the contact line crosses the creek running
through that village at just about or near Ogden Center, and
follows approximately the 600 foot contour line. To the west
the topography indicates no abrupt or noteworthy change in
the position of this line but outcrops are of very rare occurrence.
In the traverse from Adams Basin southward no other outcrops
of the Niagara shale were observed.

Lockport dolomites. Station 14. Elevation 625 feet A. T.
This is a spot on the farm of E. Arnold, township of Ogden
just east of the highway leading due south from Adams Basin
where a thin, quite pure somewhat crinoidal dolomite has been
taken out in small quantity for local construction purposes.

- Station 13. At the four corners du re south h of s
a field to east of road is an outerop of gray, § ome ewh
dolomite, 3 feet. Elevation on topographic shee bea ee
ately the same as that of station 14, the stratum | |
close on that exposed at former station. irhase’a cr ra
mites carrying some silicious nodules and silicified fos 0
sites, Stromatopora, etc.), their roughened curfseel
unequal weathering, are exposed at various points to - t] he eas
and west of this road north and south of the hamlet of Og
and from the elevation stated where they immediately ¢ : rerhie
the rock at station 15, through an interval of about - veg
These outcrops are also to be observed freely throughout | the
region east and west, specially along the first east and y we est
road north of the Ogden road, and from there westward. ee ¥
Stations 12, 11, 10, 6, 5 and 4. These very characteristic
scraggy dolomites vary little in texture and color. For ‘the.
most part the outcrops show the usual rough surface with one
siderable chert often replacing the corals but so far as observed
other fossils than corals or Stromatopora are seldom present. —
Here and there, as at station 11 on the north and south road —
the first east of the Ogden-Churchville highway, the rocks have —
a smoother, more homogeneous character and carry less chert. _
This layer however appears to be one. intercalated het weal
other layers of the more silicious material. Similar exposures —
of these dolomites indicated for the most part by boulders a
loose above concealed outcrops, are to be seen over the terri- .
tory to the west, approximately along the boundary line —
between the towns of Bergen and Sweden.
Salina beds. The lower limit of the Salina in this section is
indicated by an outcrop on the road from Churchville to North —

- 2 Je

= Chili. is peered by Seah coated (station 8) just south
4 of Churchville village in drain excavations on the Riga road.
Also along the banks of Black creek at station 7, near the con-

a -Alvence with a branch from the west, 1 mile south of Church-

4 * ville, where are 15 feet of mottled red green and gray shales.
At station 1, 3 miles southeast of Churchville, 15 feet of green-

q ish and gray shales are exposed on both sides of the creek and

5 extend in interrupted exposures as far as the road to Buckbee

Corners, crossing the creek. Thus it is evident that the region

north of Black creek to the last outcrop of the Lockport dolo-
mite, a distance of 3 miles, is covered by the soft shales of the
basal portion of the Salina.

Albion quadrangle. Medina sandstone. Holley. The extensive
quarries in the Medina sandstone about Holley and the sec:
tions afforded along the banks of Sandy creek coming in from
the south, give an instructive exhibit of the character and varia-
tions in this formation. Along the banks of the creek to the
north of the town (station 22) are banks of red and green shale
‘15 feet thick and the lower sandstones are exposed in rather
thin red and brownish beds much mottled and interlaminated
with white, but with a single heavy homogeneous red layer at
the bottom. At a quarry near the towpath at the crossing of
the first north-south road east of the village, above the red

wee A EDR dase

cet
;

and along the escarpment meee Scag oranch
creek are noteworthy exposures of Clinton sere
ing from just north of the village to 14 miles to the s'

Other exposures of Clinton limestone were not ob serv
the topography soon becomes depressed so that the ex
Rochester shales are, so far as our obseryations ext
this section, concealed. Kae

Lockport dolomites. At about 1} miles south of the —
served exposure of the Clinton limestone, just north of pa .
tlement known as Honest Hill, and to the west of the k es =
leading to Byron, is a small quarry on the Arnold farm f
which thin slabs of gray, comparatively pure or slig] )
dolomitic limestone have been taken and this rock seems tone =
tain to the base of the Lockport dolomitic series. The country ‘
here enters the eastern arm of the Oak Orchard swamp and- a
other outcrops are here concealed, the only additional evidence — E..
of the presence of the dolomite series being found at the south
‘edge of this swamp land where occasional accumulations of the 2
scraggy upper dolomites are to be observed. At one point just
north of Pumpkin hill on a northerly branch of Black creek
these layers were at one time brought together and burned for
lime, the kiln and piles of accumulated material still being in
evidence. After passing the probable southern limit of the
dolomite area approximately along the course of Black creek,
the country becomes so low and marshy, specially to the east
in the direction of Bergen, that no outcrops are afforded
and from Byron to Elba a distance of 64 miles, and from Elba
north to Langton Corners, 1 mile, and from there north 14 miles
to the east and over various points along that road southward
to East Oakfield and thence to Oakfield village, no outcrop could

=

iS
a
q
‘«
z
:
|
.
j

- REPORT OF THE STATE PALEONTOLOGIST 1901 21

E be. ascertained at any place. For this area we are therefore
compelled to construct from the data brought together from
_ the adjoining territory the probable contact lines, clearly in-

dicated in some places by actual exposures and suggested with
strong probability in others.

Medina quadrangle. The country forming the south boundary
of the Oak Orchard and Tonawanda creek swamps is likewise
barren of any trace of outcrop. .The region was carefully
traversed from Oakfield, where the gypsum beds of the Salina
are extensively wrought, 3 miles to Bumpus triangulation sta-
tion, thence west to Wheatville, Alabama and West Alabama,
south to South Alabama and Smithville station. It is appro-
priate to note from the conditions here displayed by the
topography that the great swamp area which extends entirely

across this Medina quadrangle rests on the excavated Salina

shales or the dolomite series beneath, from which the shales

have been removed.

North from the Tonawanda reservation along the drainage
eanal running into Oak Orchard creek at a point from 1} to 1
mile south of Shelby where this channel was excavated through
the rock, are expased a succession of the Lockport dolomites.

Station 27. Where the first east and west road south of
Shelby crosses the creek, the lower rock is a bluish gray dolo-
mite weathering brown, in thin rough layers from 3-12 inches
thick. Fossils occur in this rock, most abundant of which are
Zaphrentis and other corals, with Stromatopora. Above this
is a band of coarse grained dark dolomite 4 feet thick, some of
the layers of which are quite soft and shaly. Here also are
found small corals. At the top of this band is a well defined
change in the character of the deposition, the rock becoming a
more compact and more heavily bedded brown scraggy dolomite.
6 to 8 feet of this rock are exposed along the creek for a total
distance of about a half mile, and a very large amount taken
from the channel six or eight years ago is piled up in heaps on
the banks. Just above the bridges on the north and south road
the rock dips below the bottom of the excavation but is brought

oo

e paren enneey ctr :

‘middle of the bluff, and just below on the face of the e

Behe sioan ie See Or
Rochester shale. Station 28. dint ,

port limestone of which about 30 feet are seen ee
These beds are very close on the base of the limesto
for at a short distance farther down the stream is an ¢ a
the upper Rochester shale bearing a 1 foot silicious bed

ment which is indicated by the 600 foot contour line « f
topographic map is a clean cut exposure of this shale. — ie re
Clinton beds. Station 29. No further outcrop is seen along
the course of the creek till the southern outskirts of Medina —
village are reached where (station 30) is an outcrop on the creek
bank 3 mile north of the dam, exposing crystalline crinoidal > ;
limestone with well defined Clinton fossils. e° ™

Medina sandstone. A few rods farther down (station 31) the o
creek exposes a white greenish coarse sandstone of the upper
Medina, and from there north Medina sandstone exposures are
of frequent occurrence throughout the region. From these ob-
servations we have the means of identifying with approximate
accuracy the contact lines of the Medina-Clinton, Clinton-Roch-
ester and Rochester-Lockport beds.

Relation of the Oak Orchard swamp to these rock formations. A
map of sufficient size such as the topographic sheets of Albion
and Medina indicating the extent and distribution of the swamp
areas in this region, shows that one can not ascribe to any
lithologic differences in these formations a sufficient cause for
the present area of these swamps. The marsh along the course
of Black creek between Byron and Bergen doubtless lies on the
Salina shales or is underlain by a pavement of Lockport dolo-
mite where those shales have been removed. But we observe

Ea ey awe )

REPORT OF THE STATE PALEONTOLOGIST 1901 523,

' over the area which must be ascribed to the exposures of Lock-

port dolomites where at least the dolomites must be in main
the underlying rock, the considerable, often thin, broken and
interrupted extensions of the swamp areas. The rock ridge
showing just north of Churchville and North Chili thence west-
ward beyond Shelby, a ridge composed of the Lockport dolo-
mites, may hold the key to the artificial drainage of the major
Swamp areas. The great body of the swamp north and south
covers not only the width of the Lockport dolomite but also
that of the Rochester shale and extends farther to the north
than it is proper to draw the dividing line between the Clinton
and Medina. From this consideration then it becomes evident
that the heterogeneous character and the differential erosion of
the underlying rocks are not a sufficient cause for the present
distribution of the swamp areas, and while this is doubtless
an efficient contributory cause for the actual existence of these

extensive depressions, their original boundary has been exag-

gerated by artificial obstruction to drainage.

- of'the U. 8. peotenieal survey ‘during the se
‘tions were carried on mainly by Prof. L. ©. |
assistance of Charles Butts. Mr Butts was:
cerned in the collection of paleontologic data from rail
stratigraphic horizons and the careful study and de 7 mina
of material accumulated by him has led toa pretty ¢
standing of the succession of the faunas in the district.
been well understood that the lower lands of the =
underlain by rocks which could be referred without qu
the upper layers of the Chemung formation but the str
ping the hills of the southern portion of the area have
variously referred to the Devonic and in part to the lowest t
of the Carbonic. The vagueness of this reference and the w
of any recognized line of division between accepted Devonic and ce
supposed Carbonic has been due partly to lack of requisite
study and partly to the gradual and undisturbed succession of =
sedimentation. Between what has heretofore been supposed 3
to be Carbonic (without taking into account any more exact —
denomination of the horizon) and the recognized Chemung a
is a series of beds which has been usually termed Cats Ya
kill and in part so represented on the geologic maps of the state. &
One of the direct purposes of this work was to determine the

value of these beds over an interval where a passage from one
of the great paleozoic systems into another was clearly to be |
looked for. That there is no Catskill sedimentation here in the a
true meaning of the word, i.e. Catskill in the sense of implying 7
estuarine sedimentation with distinctive organisms of fresh or
brackish water habit such as occur in the typical section of
eastern New York, is made quite probable. In a general way
the section of sediments from north to south across this sheet —

waa

REPORT OF THE STATE PALEONTOLOGIST 1901 525

~

is represented by the accompanying diagram where the strata

are numbered from top to bottom by the figures 1-13 inclusive.
The region is a country of sandstones and flags with interbedded
conglomerates and the nature of these beds is sufficiently

explained in the matter on the diagram. It will be noted that
in this series there are two well defined and heavy sandstones

and two equally conspicuous and heavy conglomerates. The
Jowest of these sandstone beds is stratum no. 13, the Cuba
sandstone. 600 feet above it lies stratum no. 8, the Wolf creek
conglomerate. Above the latter 200 feet, is the Mount Hermon
or Salamanca conglomerate, no. 6, and from there the section
rises about 200 feet to the Olean conglomerate, no. 2; the high-
est sediment in the series being the calcareous shales lying on
the top of the last named conglomerate which has been termed
the Olean shale. Intervening between the Wolf creek con-
glomerate and the Mount Hermon sandstone the beds are red

_ and green shales interbedded with

flagey sands, to which it has been
proposed to apply the term Cat-
taraugus beds. The validity and

usefulness of.the distinctive term Mt. Hermon or

Salmanaca cdl.
for these strata which represent

Wolf creek cal.
those at times referred to the
Catskill formation because of
their red color and doubtless a
western continuation of Catskill
sedimentation is very clearly in-
dicated by the paleontologic eyvi-
dence which they have furnished.
For the shales above the Mount
Hermon sandstone and thence to

Cuba sndstn

the base of the Olean conglomerate it has been suggested that
still another distinctive term would be required, but it is not.
clear that stratigraphic evidence would favor such determina-
tion. The propriety of the subdivision could be established by
the variation in the fossil contents, should this appear to be of

i. ra ~3 .
for mer _ which proves to be

en succession of the faunas. It i is ane am

evidence in this undisturbed and un region |
change by sudden extinction of species or ees une exy
from east or west, but the succession has gone ony
ruption and it is only at that horizon where a decic i :
becomes noticeable without the extinction of ally or a
forms. q
1 Up to the Wolf creek conglomerate the common Ch 2
species seem to prevail. For example, Spir ifer di si Dy:
tus, Athyris angelica, A. cora, Chonete: Cx
scitula, Orthis tioga, Orthothetes chemung zs
ensis, Productellas of various species, Mytilarea, Nu € ula e
bellistriatra, Aviculopectens, Crenipectens, Edmondi ae
some of the Leptodesmas such as L. potens and ran :
juvenis, L. mortoni, L. sociale, Pterinopecten,
some of the gastropods like Bellerophon maera,
Euomphalus hecale, Macrochilina and the Dictyane 4
sponges. :
2 Some characteristic Chemung species pass this limit. Thus,
for example, Spirifer disjunectus, which is usually re- #
garded as an index fossil of upper Devonic time, extends beyond
the Wolf creek conglomerate up to and within the shales
beneath the Olean conglomerate, becoming however of very rare ve
_occurrence in horizons above no. 8. Camaro toechia .
contracta is recorded from all horizons from the base up
to and into the Mount Hermon or Salamanca conglomerate.
Such species as these however, of which we have cited the most
striking instances, must be looked on in the face of the rest
of the evidence as having their value as diagnostic of Devonic
time modified by the introduction before their extinction of a

rad

3e ford shales of Ohio, appears here and also in the overlying
BAC:
Pe: at iola pr aecedens ae a considerable number of
he Ptychopterias; some are identifiable with previously known
f ‘species and others appear to be of variant form. Witha single
| — doubtful exception all these Ptychopterias appear at this hori-
z zon or above it. Palaeanatina typa also makes its ap-
pearance here. The effect however of this conglomerate in the
strata is less marked in this respect as the point of departure of
novel forms of the series than as a dividing line in the succes-

sion of faunas. We may indicate the contrast in the aspect of

the faunas above and below this line by the following columns:

Above base of Wolf creek conglomerate

7
Agelacrinus buttsi |

Below base of Wolf creek conglomerate *
Athyris angelica
a : A. cora
oe. A. polita
Camarotoechia allegania
Chonetes scitula

Oehlertella pleurites

Schizophoria 2 sp.
k. 2 Productella 5 sp.
a | Edmondia 3 sp.
g Leptodesma potens
| «var, juvenis

; rs mortoni

j # aS sociale

| - matheri
“ longispinum
RS protextum
" spinigerum

oo 8 sp. . ae se ne
_ Palaeanatina 2 sp. .

Bothriolepis

~ Ctenodus
Holoptychius | Prine ictya 2
Gyracanthus , | Thysanotitya 2 sp.
Fishes | -

It becomes quite clear that a Hine aeal ch _ nge h
entered on the nature of the fauna with the depositi ‘
Wolf creek conglomerate and in the species ore co m menc-
ing their existence we find a certain well defined aspect of = =e
bonic life, the presence of which is supplemented by the a
disappearance of the leading features of the Chemung tao na. a
We have made special reference to Oehlertella ee
rites and have already in another place discussed the ete,
acters of the Agelacrinites buttsi from the stratum5 —
which shows a close affinity to cystids of the early Carbonic. Be q
It is to be further noted that the post or supra-Carbonic aspect — ‘4
is indicated by the Ptychopterias and Pararcas rather than a—
true Devonic though the presence of heraldic forms of these i
genera in Devonic strata is not to be questioned. Yet here by
their profusion they indicate a faunal aspect which is peculiar ©
to this horizon. Attention may be directed to the presence of
fish remains which have been found in the red beds of stratum
no. 7, and of them some, like Holoptychius ameri-
canus, may be regarded as suggesting the horizon of the Cats-
kill of eastern New York, while others, Gyracanthus, Cteno-
dotus and Bothriolepis point with more definiteness to a higher
horizon.

E

r “THE POTSDAM SANDSTONE OF THE LAKE CHAMPLAIN

BASIN
NOTES ON FIELD WORK 1901
WIIH MAP

BY GILBERT VAN INGEN

The Potsdam sandstone of northern New York is, in the
bibliographic sense, one of the best known members of the
geologic column. For many years it was ‘considered the lowest
member of the series of sedimentary rocks, and was, ‘as such,
supposed to contain the oldest known representatives of
organic life. In this relation the description of the formation
was given considerable prominence in textbooks and its name
became a familiar one to students of natural history. In view
of these facts it is a matter of surprise that there is at hand

-so little definite information regarding the physical and biologic

characteristics of this formation, which is in reality the least
known element of the sedimentary series of New York. Since
the original description of the formation by Emmons in 1837-48
little has been added to our knowledge of it as developed within
the boundaries of this state. Logan! described with consider-
able detail the group as developed in its northward extension
into Canada and added several items of interest to those noted
by Emmons. Walcott? gives a few notes on the relations of
the Potsdam to the overlying formations in the vicinity of
Saratoga and Washington counties. Again in 1891 Walcott
briefly describes several sections through the formation along
the northern and eastern flanks of the Adirondack mountains,
in which are given the thickness of the deposits, general state-
ments on the character of the materials, and in which certain
fossiliferous zones are recognized as occurring at horizous in
the upper part of the series. Ells, 1894, in a paper on the
Potsdam and Beekmantown formations of Quebec and eastern
Ontario, describes the transition from the sandstone of the

*Geology of Canada. 1863. p. 87-96.
*U. S. geol. survey. Bul. 30. 1886. p. 21.

stone at several localities on 1 the: . northeaste

(OMB Sey et
+ 5 t

ase wes cue bo a
~ descriptions of the physica

Adirondacks. The reports on the geology of ee :
of the mountains along the shore of Lake Cha: we
little more than descriptions of the areal. distributi
sandstone. AS

Some descriptions of fossils found in the formation
published, in nearly all cases however without reterends et 0 he
particular horizons within the formation from which hey were
obtained. Walcott’s sections are the only description: Fines nt )
in which the fossils are referred to definite horizons | |
sections. | | 2 ic e r

The above statements will indicate that up to the | Dr igi i *
time no systematic attempt has been made to study the form: o
tion in its entirety throughout its distribution round the west 4
ern, northern and eastern slopes of the Adirondacks and as as
result the following questions remain entirely or in great part
unanswered. T a

1 What are the relations of the Potsdam to the subjacent as
formations, whether the latter be of pre-Cambric or lower Cam- 3
bric age? Ming

2 What are the relations of the Potsdam to the superjacent
beds of the lower Champlainic (Siluric) series?

3 Where shall the upper limit of the Potsdam be drawn?

4 What are the physical characters that may serve aS &@ ~
means of distinguishing the lower from the middle and upper | §
portions of the Potsdam sandstone?

5 What are the fossil contents of the Potsdam and may they
be grouped to form distinct biologic zones? To what extent
are they reliable as a means of subdividing the formation and —
recognizing the lower, middle and upper portions?

4

REPORT OF THE STATE PALEONTOLOGIST 1901 581

= 6 The Potsdam sandstone being a litoral deposit, what is its
_ deeper water facies?
a: At the request of the state paleontologist and with a view to
‘securing information toward a solution of some of the above
g - mentioned problems, field work was commenced in the vicinity
of Plattsburg, Clinton co. and extended southward through the
towns of Plattsburg, Schuyler Falls, Peru and Ausable, into
Chesterfield, Essex co. Special trips were also made to Wills-
boro and Crown Point, Essex co. in the vicinity of which villages
the Potsdam has been described as exposed in close proximity
to beds of the overlying Beekmantown series. Northward
from Plattsburg the work has been continued into the towns of
Beekmantown, Chazy, and Champlain.

The following sections, brief synopses of which are given, have
been examined with care.

Valley of the Saranac river from above Cadyville to its mouth
at Plattsburg, a distance of 10 miles.

Valley of Salmon river from Peaseleeville to its mouth, 11
miles. :

Valley of Little Ausable river from above Peru to its mouth,
7 miles.

Valley of Dry Mill brook near Valcour, 3 miles.

Valley of Ausable river from above Keeseyille, through
Ausable chasm, about 4 miles.

Valley of Boquet river at Willsboro from village to lake and
along lake shore, total 5 miles.

Railroad cut along D. & H. track at Burdick’s crossing north
of Crown Point, about 14 miles.

Synopsis of sections
Saranac river section from near Cadyville to its mouth at Platts-
burg, length about 10 miles

General strike of beds north with an easterly dip of from
5°-10°. Direction of section easterly. Formations Potsdam
to Trenton.

This section is described somewhat in detail as it serves as
typical of the middle and upper portions of the Potsdam forma.
tion of this vicinity.

°

Skoptegarey eps

a Saale phim of 5 ation is pti Sy. arift d
it is impossible to determine how much of the ¢ |
lain by Potsdam sandstone and how much by the 1 3eekn
town beds. Still farther down the river, 2} miles, tl
limestone, 127-A4, outcrops in the river bed with the § same
eral easterly dip. A short distance beyond the Chazy 0 .) uter¢ 08
the Trenton limestone appears in the stream and continues 0
the lake shore. Throughout the entire section the strike an nd —
dip has little variation; the strike changing from N 15° W to ;
N 15° E, and the dip from 5° to 10° degrees easterly. ‘There is. -
no evidence of faulting to increase the apparent thickness 0 ti
the deposits by duplication of beds. Computing from the
length of section, strike and dip, and difference in altitude st
between the exposure of lowest layer and that of highest layer,
we obtain from the Potsdam an estimated thickness of 1150 —
feet, of which amount the upper 350 feet is fossiliferous. gf !

The lower portions of the formation as seen in this section | a

a. >
~S- -

are of light color; generally gray, with variations to yellowish ex:
and bluish gray and occasionally pink tints. The material is
quartz sand, well cemented with silicious cement, the grains
being both angular and somewhat rounded and varying in size — |
from j-2mm, with grains of 4 mm diameter on the surfaces _
of some layers. Many layers contain a considerable admixture a
of small grains of partly kaolinized feldspar. The layers vary a
in thickness from 6-24 inches and are as a rule quite compact.
Ripple-marks are common on the surfaces of beds and cross-
bedding is seen in nearly all layers. A few layers have thin
pebbles of shaly material on their upper surfaces, but no

vin
2

-

~

REPORT OF THE STATE PALEONTOLOGIST 1901 533

: _ shale pebbles were seen embedded in the midst of layers in this
= portion of the section. No traces of fossils were found.

aa This description applies to the rock as exposed at the Ellis
dam and just below “ Mill C” of the International paper co.,
14 miles down the river, and also to the lower part of the sec-
tion at Kent Falls, 125-A1.

The upper and fossiliferous portion of the sandstone in this
section as seen at Kent Falls, 125-A2 to 13, differs in several
important respects from the lower barren portion. The upper

part has many layers of thinly bedded, greenish, argillaceous
sandstone with shaly partings, on which are fucoids and worm
trails. Other layers contain pebbles of shale and dolomite and
in these layers are usually found the fossils, which consist of
trilobites, brachiopods and gastropods. These upper layers
are also wanting in feldspar. The sand grains of which they
are made up are markedly rounder, and as a rule the cementa-
tion is not so thorough as it is in the lower beds. Heavy beds
of compact, even grained, sandstone are less frequent than
below. |

The uppermost layer of this section is a heavy bed, 10 feet
thick, of white, granular, quartz sandstone, with ripple-marked
surface, and cross-bedded section. Its appearance is totally dif-
ferent from the heavy beds of the lower portion, its grains
being slightly larger, more rounded, and less closely cemented,
so that the rock crumbles readily under the blow of a hammer.

Synopsis of the Kent Falls section to show order of fossiliferous
horizons, from below upward

125-A1l Barren sandstone 30 feet

125-A2 Irregularly bedded sandstone, shale partings;
Lingulella and Obolella ) feet

125-A3 Barren sandstone 25 feet

125-A4 Bluish sandstone thinly laminated; Lingulella
_ abundant 5 feet

125-A5 Heavy sandstone; Scolithus linearis
abundant 3 feet

thinner laminae. | :
choparia miowean? ee cep
alites verrucosus, in abundance —
125-A8 Sandstone thinly bedded and shaly in lowe
portion, heavy in upper portion; Li n ig u-
loid fragments in abundance in lower por a

tion , Tee
125-A9a Vertical interval unknown Abo fee
125-A9b Thinly bedded sandstone with fucoids and “ae
ripple-marks ms et

125-A10 Irregularly bedded sandstone with pebbles andes =f
cavities; laminae separated by shaly part:
ings; fossils most abundant near middle bed;
Conocephalites verrucosus(?); o)
Ptychoparia minuta(?), Lingulella,
Obolella, worm borings, fucoids .
125-A1l Light colored thinly bedded, coarse grained
sandstone, full of cavities due to solution of
embedded pebbles; fossils, Trilobites (three
species), Ophileta, Platyéeras, Obolella, Lin-
gulella,Scolithus canadensis. This
fauna has a Siluric expression in the pres-
ence of the two gastropods, Ophileta and
Platyceras
125-A2 Vertical interval unknown
125-A13 Granular, white quartz sandstone forming
highest bed of this section; no fossils; ripple-
marked and cross-bedded. 5
The Beekmantown dolomite, 127-B1-3, appears first in bed
of Saranac river at Treadwell’s mill, 5 miles below Kent Falls, 4

nih Me, ee Sipte 1 ae i : be
e rT a i j v1 a te ee ere ee
a A ’ a & Meee
:*) vu ee Pe ee ran it

Te et Cae eee ee eee a e

t y -arenaceous, Sati numerous geodes ae ela and oe

ion finding any.
Rdenani river section

The elevated land to the west of Peru and einen Mills, -

and to the southeast of Peaseleeville is due to the resistant
S character of the heavy beds of the lower portion of the Potsdam ~

sandstone which covers the eastern slope of the gneissoid hill
known as Terry mountain. The sandstone has a very thin
covering of soil and drift and is exposed along the roads that

traverse this region, which is locally known as “ The Patent”.

These outcrops of the lower Potsdam, 129-Aol1, consist of ledges

_ of coarse grained quartz sandstone with a considerable admix-
ture of fresh, nonkaolinized feldspar. In color the rock varies

from white to gray, yellow, and red. Ripple-marks and cross- —
bedding are common. No traces of fossils were found. Owing

‘ to the irregularity of the ground it was impossible to measure

a section across this region. The general strike is northwest,
with a dip of 5° or less to the northeast.
This portion of the sandstone belongs apparently at a much

~ lower horizon in the formation than does that at Ellis dam on

Saranac river.

Higher layers of the Potsdam are exposed at the mill dam
and at the site of the old forge on the Salmon river at Norris-
ville, 15 miles northeast of the exposures of 129-Aol on “ The
Parent”. 3

At Norrisville, white sandstone, 129-Ao, 30 feet thick, is seen
in the small gorge of Salmon river. The rock is heavily bedded
in layers 2-3 feet thick, with much ripple-marking and cross-
bedding, but with neither pebbles nor fossils, and has a diminish-
ing amount of feldspar.

mo traces of pte were found in any part of it. oe ae

YS conn Lingulella ie pia ay:

ape. oT ; nt, . “
rey Med
ote, fe Sos 2, Den of eo a, f %
vi : ‘ J ¥: Dh ?, : ‘

z ~, " - ow
“ca bedde zn peg aL
¢ it LU.

a

_ bearing bed, 125-A2, of the Kent 1 ‘alls section. —
No higher beds of the Potsdam are seen above th
ler Falls; the next exposure being of the Beekmanto
with Ophileta and Lingula fragments, in the river
crossing of the Salmon river road at South Plattsbu: on ie
to the east. Re

Little Ausable river section from Peru to mouth of ri

At the road-crossing in the village of Peru the Beek
dolomite appears in the bed of the river below both i
and lower dams. From this point the river flows approximately —
along the strike of the beds to the northeast for 1} ae O 2
Lapham Mills, where its course changes to southeast cand it
flows over ledges of Potsdam sandstone. e |

The sandstone at Lapham Mills, 126-C3, has a thickness ot x
about 50 feet, the exposure extending for 4 mile down the river <2 4 ‘
from the railroad bridge, and is in some respects different from
that seen at any of the other localities. The rock is generally
a coarse sandstone of gray color with many layers of brown and — ‘
red. These red layers are of great hardness and glassy frac-
ture, and full of large grains of pellucid quartz that often attain

a diameter of $ inch. Ripple-marks and cross-bedding are

He
ie

common. No traces whatever of fossils.

One half mile farther down the river in an easterly direction is —
another exposure of Potsdam, 126-C2, forming ledges in the
river bed. <A total thickness of 10 feet is shown. The bedding
is very irregular, the layers varying from 1-4 inches in thickness,
often with shaly partings. The color ranges from white to gray,
greenish, and brown; and the texture from fine to coarse. Some
layers contain pebbles of schist and s!ate that attain sizes of 1-3

erminable fossils have been found in any of these dolomites |
and it is Bom impossible to place them in any particular division

as of the series. It is also at present impracticable to determine

q their relations to the neighboring Potsdam. The strikes and
q i dips of the separate exposures correspond sufficiently to allow
a = the assumption that the two formations are here in their normal

order of superposition. Other facts, however, seem to point to
_adifferent relation. The outcrops are far apart, } mile at least;

q and only 3 miles to the southward the two formations are

—-
a

¥
im
_

faulted against each other. The lithic characters of the sand-

stone seem also to indicate that instead of belonging in the
upper part of the formation it should be placed below any of the
known fossiliferous horizons.

Dry Mill brook section in the town of Peru, Clinton co.

Dry Mill brook is a small stream that flows into the Ausable
river about 12 miles north of the mouth of Ausable chasm.
Just west of the crossing of Telegraph street the steel gray
Beekmantown dolomite, 150-E6, forms ledges in the field. No
fossils occur here.

Farther down the stream at the crossing of Lyon street, 13
miles to the east, the dolomite, 150-E5, is again seen in the bed
of the stream and continues from this point for 350 feet from
the road bridge. At this point the dolomite is faulted against
the Potsdam by a normal fault with downthrow to the west.
To the east the Potsdam extends for a distance of 600 feet, with
a thickness of 20 feet. The Potsdam here is a coarse sandstone
of dark color with some layers that contain black pebbles, and
a few thin layers of gray arenaceous shale. No fossils were
found init. Its horizon is unknown.

* * for some aba aa the he lak
ie rte e rock here is 20 feet thick and consists of
“bedded layers of white and gray sandstone, son
tain thin seams of black pebbles. — Ripple-m
No fossils. The rock is much broken by jue {
are bent; indications of proximity to a line a
These beds do not belong to the basal portion of the
and must be separated from the anorthosite by a fau

a a weet

Ausable river section from Keeseville through Aveda che | oe
Near the road 1 mile west of Keeseville, just beyond ‘the : : ce-
track, the base of the Potsdam sandstone, 150- E2, is seen
in a depression between two ridges of anorthosite. The al
basal contact of the sandstone can not be seen. This loce iy
was described in considerable detail by Cushing! in his” re: |

eee
mie.

port on Clinton county. The rock is here a coarse con i.
glomerate of red sandstone containing gneissic fragments at. eS .
base, overlain by red sandstone of finer grain. The rock through: _
out the entire exposure contains a large amount of feldspar.
Across the strike to the southeast the nearest exposure of the | =
sandstone is on the bank of the Ausable river, about $ mice
above Keeseville, where it, 150-B1, outcrops in the vicinity of a
boss of anorthosite on the right bank. This outcrop was men- —

tioned by Walcott (1891, p. 343), and was evidently considered :
by him the basal portion of the sandstone. In reality it is an
exposure along a fault which separates it from the anorthosite,
and the rock here belongs to a horizon quite well up in the for-

ré te

mation though just how far it is impossible to say.

From this point the sandstone is exposed at intervals for 14 .
miles to the dam of the pulp mill at Alice Falls, a short dis- — 4
tance above the head of the Ausable chasm. Throughout this
distance the beds exposed, 150-B1 to 7, are of the same char-
acter as those of the lower portion, 125-B1 to 2, and A1, of the

iN. Y. state ry 15th an. ean 1895. p. 548.

Fault; hght ine
on downthrow side

e Strike and dip

® Horizontal

JAMES 8. LYON
tate Printer

PAS
SHOWILERATA

blocks; the eae faults having a iewstion of about
>: 30° e., while the minor faults trend north and south. The
| x s¢ Bbcabince of the layers throughout the unfossiliferous
4 ortion of the sandstone series caused considerable difficulty
tn the determination of the amount of displacement of the
a faults and led to the exclusion, from the total esti-
- mate of thickness, of those beds the exact position of which
a could not be satisfactorily established.
3 The section of the chasm is through three blocks of sand-
_ stone of which the middle block has been Es ae down between
the north and the south blocks. :
The north block with a thickness of 50 feet is of uncertain re-
_ lation to the other two, so its thickness has been excluded from
the total estimate.
4 The south block extending from Devil’s Oven to Alice Falls
has a thickness of at least 210 feet. The rock of this block is
gray and white sandstone in layers of 2 inches to 3 feet thick-
ness. Ripple-marks and cross-bedding are common. The only
fossils found in the layers of this block were tracks of Cli-
mactichnites wilsoni which range through 10 feet of
_ ripple-marked layers at a horizon about 90 feet below the top
of the block. These layers are exposed at the top of the Bir-
mingham fall at the head of the chasm.
The middle block with the highest beds of this section fur-
a nished the layers containing brachiopods, trilobites and gastro-
_ pods. The thickness of this block as exposed to view is 245
feet. The lowest fossiliferous horizon is at 110 feet from the
: bottom of the block. This is a sandstone containing pebbles of

-

LEGEND

“A
Beekmantown

Potsdam

Fant; ight line

on downthrow side

Ne Strike and dip

® Horizontal

JOHN M. CLARKE
STATE PALBONTOLOGIST

UNIVERSITY OF THE STATE OF NEW YORK
NEW YORK STATE MUSEUM

ANNUAL REPORT 1901

= : SS AL Jable Cha

4 \
Ayjee Falls Fault |

BOUNDARY _

LINE

1 4

Ie

Contour Interval 20 feet

Datum ismean Sea level

JAMES B. LYON

PORTION OF S.E.CLINTON AND N.E.ESSEX COUNTIES 710"
SHOWING EXPOSURES OF POTSDAM AND BEEKMANTOWN STRATA
G. VAN INGEN. 1901

3 1
Seale 62500

minata, Obolella prima. bets .
Above this zone Lingulella and Obolelia. re a ir at f
intervals throughout 90 feet of the section to wi hin 50
of the top. No other trilobite-bearing bed, and no gastr pc
were found at higher horizons in this section and we are
to think that the highest horizon of this Ausable section
below that of the Ophileta bed of the Potsdam at Kent ie
The total estimate of the thickness of the formation a
section must fall considerably below its actual thickness Ww i
probably will never be determined because of frequent and pr
found faulting. The measured thickness is at least 455 feet, 0:
which a lower portion, 210 feet, is in the south block, and a i} ae
higher portion of 245 feet in the middle block. Of this thick- -
ness the upper 110 feet contains the typical Potsdam fauna, — -
without any indications of Siluric relationships. To this total
may be added 15 feet, the thickness of the basal beds west of
Keeseville, which brings the measured section, with exclusion —
of all doubtful beds, up to 470 feet.

a

—»

Willsboro section

The Potsdam sandstone has been reported by J. F. Kemp and >
the late T. G. White (1894), as occurring in close proximity to
the Beekmantown in the valley of the Bouquet river at the yvil-
lage of Willsboro, and on the shore of Lake Champlain near
the mouth of the river. The exposures mentioned by the above
authors were examined with the result that all the rock cropping
out in the river near the village proves to belong within the
limits of the Beekmantown series. Down the river, below the

“The Pe cnx of the Potsdam shown here is about 135 feet.

The rock is in heavy and thin beds, many layers containing
e pebbles of shale which on exposure to the atmosphere result
in the formation of cavities. Thin layers of greenish arenaceous

Shale are common. About the middle of the section is a layer,

152-A38, containing Lingulella and Obolella in abundance. No

trilobites were seen.
_ This section seems to be about equivalent with the lower por-

tion of the Kent Falls section.

Crown Point section

A section was examined along the track of the D. & H. R. R.
near Burdick’s crossing i miles north of Crown Point with the
hope of finding some trace of the Potsdam sandstone beneath
the lower layers of the Beekmantown. The search proved vain
so far as finding the Potsdam was concerned, though the lower
portions of the dolomite were found to be arenaceous. The sec-
tion is 130 feet thick, with Ophileta toward the top of the
Series. An interesting intra-formational breccia occurs in the
lower part of the section and chert beds toward the middle.

Summary of results

The area covered by the sections above described is of small
extent when compared with that over which the Potsdam sand-
stone forms the surface rock to the north and northwest; the
results obtained can, accordingly, have little more than pro-
vincial value and the conclusions drawn must be of a tentative
nature till such time as they may be confirmed after field work
over the adjoining districts. They will, however, serve to in-

—_

contact, the nature of the contact pelts ‘such. as te Oy: ir
period of long continued erosion. It is of interest on )
in some cases the materials composing the basal co ng lon
have been transported from considerable distances a: and
no fragments of the subjacent rock of the pa
Such an instance is afforded by our basal sandstone, 150-E2,
of Keeseville, a good description of which has been ali
published by Cushing. : as
No formations of Cambric age have been found below the J is
dam in the area covered by this report. Certain hypotheses. ‘sug: ai
gested by megascopic examination of the pebbles contained in
many layers of the Potsdam can not be discussed till careful
eee examinations have been made. ae m
2 A possible indication of Ordovician relationship may be”
atforded by the presence of the genus Ophileta with Platyceras — 3
in the upper part of the Kent Falls section. More extensive :
collections should be made at this point. Ta
In the area under discussion the transition beds between the ~
Potsdam and Beekmantown are absent, both by cutting out
along fault lines and by glacial erosion, drift-filled valleys ex-
tending parallel to the strike of the formation at those horizons
where *should be found the transition beds. Farther north in
the towns of Champlain and Chazy where the strike is at right
angles to the direction of movement of the continental glacier
these softer beds of the uppermost Potsdam are exposed to
view. They prove to change by slow gradations from sand.
stones with thin intercalated dolomites, through sandstones
with thicker dolomites, finally merging into dolomites with

and ‘eventually ‘te eae pur

own series. These facts are re- Bee io:

‘ Fe some extent are eo as means of recognizing ie
ian horizons.
_ he presence of feldspar grains appears to be restricted to
‘ the lower portion ; if the feldspar be accompanied by other =
= _ minerals, as magnetite, it may be taken for granted that the
i base of the formation is near at hand. Red and brown are

# “more usually the colors of the lowermost portion. Coarseness

Fs, of materials with little sorting of the grains according to sizes

are also characteristic of this portion.

a The middle portion of the sandstone is made up of well sorted

materials, of finer grain, compactly cemented, and of white,
steel gray, or yellowish color, with very little or no feldspathic
‘content. The grains of sand are both angular and rounded with
the former predominating. The layers are more regular though
their surfaces are ripple-marked, and in section they are seen
to be almost universally cross bedded. Pebbles are found on the
surfaces of some layers of the middle portion, but unlike those of
the upper portion they seem to have been of soft mud derived by
erosion of contemporaneous sediments, cast on the beach at
times of rough water and flattened and squeezed out by the
subsequent pressure and consolidation of the superimposed
sand deposits.

The upper portion of the carivatson has frequent beds of
irregular laminated sandstone with partings of greenish
arenaceous shale. The shale surfaces are covered with fucoids
and worm trails. Pebbles of shale and dolomite, which were
hardened before the time of their entombment, are found em-

bedded in the sandstone layers, and their disintegration
causes cavities to form in the layers containing them. The

A Ca

j ad tase, * beds are = camosel of nicely

under the hammer. moundea pei of r =
larger size occasionally cover the upper :
of finer grained sandstone, and being without
stand out in relief above the surface with an app
having been sprinkled from a pepper pot. In other cas
gations of noncemented grains have been found —
within layers of heavy though porous beds, as in the ¢
the Hyolithes bed, 150—A3, in the Ausable chasm.

5 No fossils have been recognized in the lower portions
the formation. The middle portion has afforded only — the:= 5
Climactichnites tracks at the Birmingham bridge, and eee Na
irregular, unidentified worm borings and trails. Ae as

The upper portion of the formation holds fossils through a.
series of beds aggregating at least 350 feet in thickness. — wees
have at present no evidence on the position of these fossil-—
iferous beds in relation to the actual top of the formation. | |
The list of fossils includes: trilobites, four species; brachio- ey
pods, three species; gastropods, three species; annelids, two
species, and several undeterminable burrows and _ trails;
fucoids, several; tracks, one species of Climactichnites.

To some extent these fossils may be arranged in zones. Such
arrangement can only be tentative and will certainly need
readjustment with the extension of the field work over a_
larger area. Two species of brachiopods, Lingulella
acuminata and Obolella prima, seem to occur
throughout the entire range of the fossiliferous horizons, as
do also the fucoids and many worm trails and branching
burrows.

iy

all Ae te

ee, eS Ye

Lingulelta a

ioe ‘Obolella | eres ‘Conrad.

= a Sy ensis Billings.
a canadensis in abundance on the upper
“Gh surfaces of sandstone layers of the transition beds in the
er uppermost portion of the formation. These uppermost
ie layers have up to the present yielded no other fossils than
; this worm burrow.
6 No answer can at present be given to this question. Some

‘suggestive evidence has been derived from the pebbles included
in the layers of sandstone at various horizons in the forma-_
tion. It is, however, of such disconnected character and

meager amount as to warrant its exclusion from the present |

a discussion.

os ae ere
Soaks yh

pang sas sey et

¢

acti

Ri,
e

ahaat a quarter of a mile east of the small settler
as Grant Hollow in the northwestern part of Renssele

a In ascending the Deep kill valley from Grant Hollo 07
first exposure is a small outcrop in the south bank of a
feet of deep black mudstone giving conchoidal fracture, )
rock has furnished no fossils. Another outcrop, wh ae
exposed somewhat contorted dark gray, sandy, thinly | bed dded |

aes

shales with a few intercalations of argillaceous sandstone, ‘is ‘a
30 feet farther up. These strata also proved to be barren pr
organisms. be* oa

The continuous section begins 700 feet farthecs east, on the
north side of the creek. The beds of this exposure are, in con-_ ;
trast to those met with farther up and down the creek, free from 3
flexures and dip uniformly N 116° E at an angle of 24°. It is
apparent that the extremely heavy bedded, hard silicious beds |
and the limestones prevailing in this section protected the
shales from being thrown into the many small, closely packed
folds so characteristic of the softer and more pliable terranes
of the region. There is no cleavage in these beds; and the
slickensides, which often run subparallel to the bedding planes
and obliterate or at least distort all organic remains in so many
outcrops of the Trenton, Utica and Lorraine shales in the Hud-
son river region, are frequent only where the heavy quartzose
banks have slipped along the thin shale partings. To the

absence of these antagonists of the paleontologist the beautiful

"408 = Ul] + pepuozoy pure [PIAA a] PIS pag a — 3
; eyo EE
) $nj PpUapP snp euSo/diy WIM QUOZ : JTaUo7Z

5 eveysau) Pa :puese7

‘ogo snpiyig sngdeSoudpyy Ypim au0z.: J auoz

auoz~ snjdeiseayjay :1 2U0Z

‘09 davjassuayy ‘I"y daeq Suoje uolaec

6 9481d

oa -_ appear ated.

oe 4 This stratum is overlain by 8 foes of thin, dark greenish
gray, hard silicious bands with thin intercalations of black
shale. The latter contain graptolites in great number. This
bed we connote as graptolite bed 1.
-e Thin bedded shales and silicious layers; 1 foot 8 schon
The lowest is a thin limestone band; another is found near the

_ middle. The silicious bands change in places to grits and

breccias as in stratum ¢. Fossils seem to be absent.

f Greenish gray, hard silicious layers and intercalated deep
black shales, forming a stratum which lithologically is like
stratum d; 1 foot 9 inches. Like the latter, it carries grapto-
lites in great profusion. Indeed, this bed has proved the richest
of all in these fossils, and its graptolites are in the best state
of preservation. It is here termed graptolite bed 2. The green-
ish quartzose bands are perforated in all directions by worm
tubes and are covered by carbonaceous blotches apparently
originating from seaweeds. _

g Thin bedded, very hard, eray to black silicious beds, 2 feet
9 inches, overlie these graptolite shales. They are not separated
by shale partings, and show no traces of organic life.

h Thin bedded, dark gray, hard limestone, with no indications
of organisms but worm tubes ; 14 feet 3 inches. The layers
possess very uneven surfaces, as if deposited in turbulent water,

—

) lists of fossils, is so different ee) it} he t alds the appea 7
a new zone. This is graptolite bed 3. ra ff 7
j Regular alternations of estan gray, thinly 1é mina
silicious layers and dark gray sandy shales; 5 feet A
no fossils. A thin seam of bluish black pyritiferou
with a few graptolites was observed both near the bot tc
top of the layers. The prapienier de net differ from t
bed 3. | Hg aa e
k Dark gray limestone cent 5 feet 9 inches. The o Himeste
layers are thin, partly evenly bedded, partly exhibiting nter- ae
locking, narrowly undulating surfaces, very similar to = mi
of the European triassic “ Wellenkalk.” There is here also ¢
breccia 5 inches thick, with coarse sand as cement. The
shaly partings between the limestone layers contain no a
tolites. “a
1 Alternations of greenish silicious beds and black shales,
with a 4 inch limestone breccia in the middle; 16 inches.
Graptolites occur sparingly and in poor state of preservation — a
in the shale. This graptolite bed 4 has the characteristic
species in common with bed 3.
m Limestones which exhibit the undulating character noted
above still more strikingly; 16 feet. The thin shale partings | :
between the limestone layers, as in all other limestone strata .
of the section, are destitute of graptolites. 7
n Covered; 8 feet 9 inches.
o This short break in the section is followed by the large
exposure in the quarry lately opened to obtain the material for
the construction of the dam of the Lansingburg waterworks.

y Ges, specimens of Phyllograptus.

which are often densely covered with graptolites,
The graptolite layers of

S the quarry beds are, on the diagram, designated by heavier
SS lines and the letter p. They constitute graptolite bed 5. By >
ie “orogenic disturbances which have affected this region the
ae blocks have been slipped along many of the partings and the

¢ fet

~

—- eo a eon = (ute (es ee
7 “* ?e

organisms destroyed. In the silicious layers only worm tubes
were noticed.

_q Here ends the practically continuous section of the natant
and middle graptolite zones, and for a distance of about 825

feet. (figure obtained by pacing) no further exposures could be

found.

ry Then follows the large but temporary exposure afforded by
the cutting into the north bank of the creek for the purpose of
securing the north end of the dam. The length of this section

-was 155 feet. The prevailing rock of the exposure was green-

ish gray quartzite, similar to that of the quarry beds, but less
compact and softer, with some brecciated layers and several
thin bands of gray limestone interbedded with the greenish
rocks. All these strata were however contorted in the manner
mentioned before.

Two graptolite beds were found in this part of the section.
The first (bed 6), 839 feet from the west end of the cut, forms
the nucleus of a narrow steep fold consisting of 6 feet of a
compact mud rock. As the bed is folded on itself, the actual
thickness of the layer is 3 feet. 30 feet farther east 2 feet of a
soft black graptolite shale were found (graptolite bed 7). On
account of the disturbed position of the beds, the exact dis-
tance between the graptolite beds and the total thickness of
the beds exposed could not be ascertained satisfactorily. The

—

to succeed that of the quarry b ‘ti
that the beds in the ares va erty, 4
lies those exposed in the lower aleeens ection.
latter there are exposed upward of 123 feet Sn ok
in the dam cut, which is 135 feet long, may have r
feet in thickness. Hence, even if the beds in the |
interval of 825 feet (which, taking account of the d a |
represent an approximate maximum of 336 feet) were. epe ae |
folded on themselves, they would easily reach 100 feet ae k-
ness, and the rocks of all three zones, from the west to t
end of the section must have attained a total fhickadaele

to 300 i

slate belt of Vermont and eastern rar York in the region t |
the north of the Deep kill have shown the occurrence in a num:
ber of localities of “dark gray calcareous or very quartzose,
finely bedded shales or black shales with thin limestone beds — Z
immediately overlying the ferruginous quartzite ” which is con- — ;
sidered of Cambric age It is added that these “are easily
overlooked on account of their inconspicuous characteristics —
and their inconsiderable thickness.” In the table facing p.

178, the latter is given as 35+ feet. Graptolites found in

these shales were referred to Dr Gurley and determined

as follows: Bryograptus, Dichograptus, Callograptus
salteri? cf. Dendrograptus sp. and Dictyonema
flabelliforme, and it was concluded that “several of
these are regarded as probably of Calciferous age.” The genera
identified indicate that either the beds observed in these locali-
ties may be identical with those of one of the Deep kill zones,

—

{Slate belt of eastern New York and western Vermont. 1899. p.185-.

' erase): ¥e. also es ares in ae slate bate cae

tolite 2 shales. The fact that the middle and upper zones
at the Deep kill seem to be absent in the outcrops re-

d to by Dale, may also sl comp t0F the small ede mic of

"that found at the Deep kill.

es A striking feature of the Deep kill section, and one worthy of
‘a “special notice, on account of the still contested nature of the
Zueuga of the graptolites, is the regular periodic succession of
the rocks associated with the black graptolite shales within
“the two lower zones. To demonstrate these cycles of depo-
4 sition, the list of the beds is given in a more comprehensive
z form. |

- a b limestones with shaly intercalations

3 “e sandy shales and grits

greenish silicious shale and black graptolite shale

sé thin bedded shales, grits and limestone

f greenish silicious shale and black graptolite shale

g greenish silicious shale

ih ee

A limestone

4a greenish silicious beds and black graptolite shale

j greenish silicious beds and sandy shales

A limestone

4 greenish silicious beds and black graptolite shale
~-m limestone

” covered

a ee ae eh bi J
'

ae

(a

- A 2.) Qe
.*

eG greenish silicious beds and black graptolite shale
It will be noticed that the deep black, soft graptolitiferous
mud shales are always inclosed in greenish gray, very hard,
thin bedded, more quartzose layers, and that between two
periods of deposition of these there is always intercalated one
of thin bedded, barren limestone. This alternation is pre-
sented five times in the section.

shales, and the absence of Bh a pastign
similar black shale partings of the aicareiia) vers4
that both the former originated under closely s: Re
tions. It suggests itself that the only change in t th
conditions was in the swiftness of the current, the s
beds being deposited in a current which carried more e
while a slackening of the current allowed the slow ¢ ies pi
of the fine argillaceous and carbonaceous mud which en 0)
the graptolitic detritus. That the latter, in most of the I De
kill beds, can not have been exposed to any turbulent mi
current action, is clearly evinced by the retention of the most — ae
delicate parts like the hydrocaulus. It is further clear that
the graptolites did not live continuously on the bottom where a
they are now found, for they appear only intermittently an@
then in vast multitudes and always in different associations. ‘3
The aspect of the paper-thin seams changes kaleidoscopically
from seam to seam; and often a surface will present nothing
but the spawn or only a certain growth stage of a single species.
These conditions of deposition, and similar ones in the Trenton
and Utica zones argue that the fauna was, from time to time,
carried into this coastal region of the sea from an outside and
presumably pelagic region.

The limestones which form considerable banks between the
graptolite beds are evidently not direct organic deposits or
shell heaps, but were either derived from the abrasion of a cal-

ie a yt

careous coast which furnished the fine calcareous mud, or were
direct chemical deposits such as are formed wherever decaying
organic matter furnishes the necessary carbonate of ammonia
to form calcium carbonate out of the gypsum contained in the
sea water. As the carbonaceous mud partings between the
calcareous layers indicate an oft-repeated interruption of the

>

=~

+ moat ee

Ravee

NTOLOGIST 1901

: ° ee In akan account of all observed Ee of deposition in the
a p "Deep kill section, it is fairly safe to conclude that an alteration

in the direction of the movement of the water caused either the
ealeareous or the silico-argillaceous mud to be deposited.

_ The fine grained shaly partings between the beds were formed
during a period of quietness; but, while these partings of the
limestone beds are barren, those of the silico-argillaceous mud
beds are covered with graptolites; hence, at the period when
the currents brought the calcareous deposits and during the
intervening shorter calms, the higher levels of that part of the
sea were free from graptolites, while at the period when the

silico-argillaceous mud was brought in, the sea swarmed with —

them.
_ In an excellent exposition! of the probable conditions of life
of the graptolites, Lapworth has concluded that the fine
‘grained black graptolitiferous sediment may have been de-
posited either in shallow or in deep water and that its forma-
tion depended not so much on depth as on the quietness of the
water. The conditions under which the Deep kill graptolite
beds appear to have been deposited seem in full accordance
with this inference, and from the character of the sediments
in that section as described above, it also appears that the
direction of the flow of the water, which precluded the period of
quietness or which continued in the higher levels of the sea
must have been on the whole shoreward from the open sea, which
latter undoubtedly was the habitat of the graptolites. Thence
they came either as holo-planktonic free floating organisms or
as pseudo-planktonic, fastened to seaweeds of the character of

_ the recent sargasso, as argued by Lapworth.
The water from which the graptolites were settling was not
altogether free of current movement, as is shown by the parallel

———

+Zeitschrift der Deutsch. geol. Gesellschaft. Jahrg. 1897. Heft 2, p.
239 ff.

xs - "3
reo =f ors eens a
ea
* ‘
-
soe

sat
t=

a

is characterized by the prevalence of valence of rey ase:
genus Didymograptus, notably of Didymey grap |
ulus, the colonies of which are found in grez E
on every slab from this bed. The entire Ais of be )
‘sists of the following forms: _ :
1 Callograptus eaiiack Hall
2 Bryograptus sp. nov.
3 Dichograptus octobrachiatus Hall” —
Tetragraptus serra Brong. (=T. bryonoiies ae ees
“ae
Hall) =
5 Tetragraptus bigsbyi Hall
6 T. fruticosus Hall
7 T. sp. nov.
8
9

rs

Didymograptus nitidus Hall
D. patulus Hall
10 Phyllograptus ilicifolius Hall
11 P. angustifolius Hall
12 Dawsonia monodon Gurley
13 Caryocaris sp.
14 Small oboloid and linguloid brachiopods
15 Small indet. gastropods

Graptolite bed no. 2

The next faunule is that of bed f, which is separated from the
preceding by only 1 foot 8 inches of barren layers. This grapto-
lite bed, with a thickness of 1 foot 9 inches, proved not only
extremely rich in number of species and specimens, but specially
valuable on account of the excellent state of preservation of

oP

ae Be

= .

= stages. ay one ae a great anes of the spconaiene yids

. pyritized, specially so the numerous hydrosomas of

Phyllograptus ilicifolius and of the dichograptids.

This material will allow an investigation into the structure of

, these forms.
ae The writer abstains in this publication from describing the
5 ‘numerous forms which are not identifiable with species hitherto

known on this continent, partly because time has not yet
allowed a satisfactory illustration nor a thorough comparison
with related species known from foreign graptolite shales; and

partly because a monograph of the graptolites of New York

is thought to furnish a more appropriate receptacle for such
descriptions. .
The following is a list of the species found in graptolite

bed 22
- Penicagtapias sp. nov. Hall

_2 Dz. ef. gracilis Hall
3 Dictyonema sp. nov.
4 Callograptus salteri Hall

a ee ee

*The peculiarity of most graptolite beds, that the separate layers of
the same bed differ in the relative prevalence of certain species and hence
in the general aspect of the assemblages, is strongly marked in this; cer-
tain layers are nearly covered with specimens of a new Bryograptus,
others with those of the various tetragraptids and again others with the
branches of dichograptids. Fossil lists of the faunules of these thin
jayers fail, however, to bring out a difference in their composition, or in
the number of species. It appears, therefore, that all these different
assemblages lying so close together in the rock, were derived from con-
temporaneous denizens of the sea. These graptolites either lived together
in sheals, or more probably, while slowly settling, became separated
according to their size and weight.

If, therefore, a form as Bryograptus sp. nov. is listed as extremely
common (cec) this statement does not refer to all layers of the bed, but
only to one or to a few.

15 T. bigsbyi Hall
16 T. quadribrachiatus Hall
17 T. aff. hicksii Hopk.
18 T. sp. nov.
t 19 T. sp. nov.
20 Phyllograptus ilicifolius Hall
21 P. angustifolius Hall
22 Didymograptus nitidus Hall
23 D. patulus Hall
24 D. extensus Hall
25 D. filiformis Tullberg
26 D. (Leptograptus) sp. nov.
27 Dawsonia tridens Gurley
28 D. monodon Gurley
29 Caryocaris curvilatus Gurley
30 Of. C. oblongus Gurley
31 Small indet. brachiopods ce
A comparison of the fauna of graptolite beds 1 and 2 proves

that both belong to the same zone. This zone is characterized — ‘Z

by the prevalence of species and individuals of the genera
Dichograptus, Tetragraptus, Didymograptus and Phyllograptus.
Of these the genus Tetragraptus appears with the greatest
number of species, and it clearly reaches the acme of its develop-
ment here. While T. quadribrachiatus and the new
species have not been observed to pass into the higher zones,

y a
3).
av

a
“7

é i]

ee” eae oe eS

=” etaptyhite zone.
Among the species of Didymograptus it is a striking oan

aa - nomenon that only the forms with horizontally extended’

branches are present, while the “ tuning fork ” species, so char-

acteristic of the middle Lower Siluric zones of Europe, are stilb

entirely absent. Goniograptus thureaui also extends
into the next zone, but does not there attain the size of its
ancestors. The genus Phyllograptus attains its largest size
(Ph. typus) and its greatest number of species only in the
next horizon. |

Nearly all the species of this fauna, which bear Hall’s name
as that of their author, were described! as coming from the
“shales of the Quebec group, Point Levis.” While Hall in these
important papers did not enter on a discussion of the age of the
graptolite shales of the Quebec group, he correlated, in the table
showing the vertical distribution of the graptolites (loc. cit. p.55),.
the Quebec group with the Calciferous and Chazy periods, thus.
placing these graptolite beds in a general way near the base
of the Lower Siluric. Nor did he attempt to separate the grap-
tolite fauna of the Quebec group into its constituent zonal
faunules, but from the associations which he mentions in the
descriptions of the species the presence of two different faunas,
that of Point Levis and that of the St Anneriver, is clearly
apparent. These two faunas were differentiated as the Point
Levis zone and the River St Anne zone by Lapworth,? and the
latter zone, in accordance with the succession established in
England, is placed above the former.

Later, the same distinguished investigator of the graptolites
Studied? collections from the lower paleozoic rocks on the south

*Geol. sur. Canada. Rep’t for 1857; and fig. and descr. Can. org. rem.
Decade 2. 1865.

Ann. and mag. nat. hist. 1880. 5th ser. 5:275.

*Roy. soc. Canada. Proc. and trans. 1886. 4:167 ff.

Ri named at ‘shout the the middle of the eries. This cone
sae verified by the actual succession: of the zones in t
A yery thorough account of the bieinepiok the prot a
Quebec terrane has been given by R. W. Ells, ace -cOm} Lerip
extensive fossil lists from all outcrops of the ‘quebel ec reg
prepared by Dr Ami. The succession of the larger d vis o : of
the Quebee terrane is therein clearly set forth. Dr | 7
cludes in this paper that the evidence afforded by the s
graphy and by the graptolites determined by Prof. Lapw
sufficient to refer the Sillery rocks (1-4) to the — Ca
system, and the Levis beds (5) to the lower Ordovician. ra a \
gests that the term “ Levis” be used for the local develop ment
of the Calciferous (Beekmantown) terrane about Quebec. TI
Levis beds measure, according to Logan, about 2000 feet i m thick
ness. As the Deep kill beds contain the greater part, if not
of the graptolites which have become known from the tae
beds, they represent a southern continuation of the same, or . 4
more exactly speaking, of the graptolite shales contained in the
Levis beds; for the conglomerate bands of the Levis region with | “=
their interesting fauna, both in the matrix and boulders, are ;
apparently wanting here.

In reviewing Dr Ells’s report, Mr Walcott? states that in
188 he found together with Dr Ells the typical Calciferous
fauna in the matrix of the conglomerate bands in the Levis beds,
while the boulders contain the Potsdam fauna. The mixing of
these two large faunas has been the cause of much of the con-
fusion and mystery surrounding for so long a time this part of
the Quebec terrane.

‘Geol. nat, hist. sur. Canada. Rep’t 1888. 2d ser. v. 3, pt 2, 12 k ff.
7Am. jour. sci. 1890. 3d ser. 39:101 ff.

4 a conditions under which the Levis beds are found in the Quebec
= Rerion, ee: not invite or permit an establishment of the succes-

os, attempt to eer this, however, by reference to the

2 eI known succession in Europe, has been made by Dr R. Gur-

per exe 2 Dr Gurley states that he had the opportunity of studying

oa es oe et aes oe aed é ae 4 a

a

_ two different collections, with different faunas, from the Point
~ Levis shales. One of these, coming from a black shale, with
Dichograptus rlexvlis and ~Phyliograptius
ilicifolius var. as conspicuous members, is termed the
Main Point Levis zone and tentatively placed in the Lower Cal-
ciferous. It is with the fauna of this zone that the assemblage _

_ described above as characterizing the lowest beds of the Deep
kill section, or those of the Tetragraptus zone, is identical.

Mr G. F. Matthew has reported? the occurrence of the zone
with Dichograptus logani and Tetragraptus
quadribrachiatus, ete. in the St John basin, separated
from the Cambric zone of Dictyonema flabelliforme
by several hundred feet (175?) of shales whose fauna is unknown.
As the other zones seem to be absent in that region, it does not
furnish any clue to the stratigraphic relations of the Levis
ZONES.

A more exact determination of the position of this zone in
the series of paleozoic formations has been possible in Scan-
dinavia and Great Britain. In England, the graptolite fauna

* Geol. soc. Am. Bul. 1890. 2: 492.
* Jour. geol. 1896.- v. 4, no. 3, p. 302.
* Can. rec. sci. Oct. 1891 > p.3; Nat. hist. soc. Bul. 10, p. 3.

* 2.
4 > ” st

sein
Bek (ne

r alia sidan ae Ol eof shea Fp rt

-noides, corresponds to the p 1e of the Q
which is the Main Point core pote Gr ei ae T
Skiddaw slates they considered as contemy p01 ral cous u te ’
lower Arenig, and therefore placed the zone near t
the lower Siluric.

Lately, the graptolite fauna of the Skiddaw slate’ E..
carefully investigated by Miss G. L. Elles Miss Ell ea con
cludes that the Skiddaw slate fauna, “though it is more ¢l closely
related to the fauna of the Quebec group of Canada tan to th ut
of any English beds, is still more nearly related to the § a
fauna; for, while of the whole 59 species, 25 are common ‘to th
Skiddaw slates and the Quebec, and only 14 common to the § Skid-
daw slates and the two other English areas, no less than mH ;
species are common to the beds of Sweden and the Skiddaw —
slates.” The fact of the greater resemblance of the Skiddaw
and Swedish faunas can not be held, however, to vitiate the con- —
clusion of the homotaxy of the Quebec or Levis and of ao 4
Skiddaw zones; for it is only natural that, in homotaxial beds ae)
the English and Swedish faunas which flourished in closely
adjoining geographic regions should have more forms in com-
mon than the Skiddaw and the far distant Levis faunas. The
writer believes that, considering the great difference in relative
distances, the great number of forms which are common to the
Skiddaw and Levis beds, and which comprise one half of all the
Skiddaw species, is as conclusive proof of the homotaxy of
these latter beds as the greater number of common species
is of the English and Swedish.beds. This argument is aided by
the consideration that the Levis fauna has not by far been as
thoroughly studied as the Skiddaw and Swedish faunas, because

> = ae

ae
-

*Quar. jour. geol. soc, 1898. 54: 463 ff.

ey

continents. Furthermore, it is just these most characteristic
- forms that are common to the Skiddaw, Swedish and Levis
- faunas. Finally, the discussion of the next two succeeding

3 - graptolite zones of the Deep kill section will show that their

-
’

succession, and hence most probably also that of the Quebec
‘zones, is identical with that of the Lake district and Scandi-

navian zones. This parallelism of the succession of the zones
can, however, be construed to mean only that these faunas

occupied these vast territories contemporaneously and in the
same succession.

The complete list of graptolites of the Skiddaw slates given
by Miss Elles (loc. cit. p. 526-27) indicates that the fauna of the
Deep kill zone, here under discussion, corresponds to a part of
the fauna of the middle Skiddaw slates or Arenig. These middle
Skiddaw slates have again been subdivided by Nicholson, Marr?
and Elles. Miss Elles divides them into the lower Tetragraptus
bed, the Dichograptus bed and the upper Tetragraptus bed. As

no lists of the faunules of these subdivisions are furnished, a

final correlation of the Deep kill Tetragraptus zone with any of
these subzones would be inadvisable at present. But the facts
that the species of the multiramose dichograptids of the genus
Clonograptus,? so common in the Main Point Levis beds, are
absent in the Deep kill zone and represented by Goniograptus, a
type of evidently later development; and that the younger genus

*Geol. mag. 1894. 4thser. 1: 122.

2In connection with the peculiar absence of species of Clonograptus may
de pointed out the equally peculiar presence of two species of Bryograptus,
4 distinctly Cambric genus; one of these with a profusion of individuals.

eo pre this ey U. “the
Fe ~ correlation is Bh gage act, that th
_ zone is homotaxial with the upper ' Te stra rapt
The investigations of Hopkinson and) Tanwar e
strated that the characteristic fossils of this zone 0 pecur |
the Arenig series of St Davids in Wales, of § shely
England, and in the Ballantrae terrane, underlying rk
series in south Scotland.

The most detailed division of the graptolitiferous has.
the most exact correlation with the limestone facies have
attained in southern Sweden where the paleozoic beds, 2
lie horizontal. It is only necessary to cite the names
narsson, Térnquist and Tullberg to indicate the refined | lin i risi¢
in zones of the Siluric in that country, which now has k
common property by its adoption in textbooks. 5 Gee

Linnarsson? comprised under the name lower Graptolite s chists se +
(or Phyllograptus schists, as proposed by Dr Térnquist) all the =
graptolite-bearing strata that lie between the Ceratopyge and ate
Orthoceras limestones. Their fauna consists of the Dichograp- sak ag
tidae and their closest ally the Phyllograptidae. He points out Pn ‘
that the most abundant species are identical with or representa-_
tive of those familiar to us in the Skiddaw and Quebee groups,
such as Didymograptus patulus, constrictus,
indentus, ete, Tetragraptus quadribrachi-
atus, bryonoides and bigsbyi. There can be, hence,
no doubt that this zone is identical with the lowest Deep kill ithe

called the Te denis zone in this publication.

—_.

* See speci ially Ann. and mag. nat. hist. 1879. 5th ser. 2:4, and Geol.
mag. 1889. 3d ser. 6:20, 59.
*Geol. Foren. Férhandl. Stockholm. 1879. no. 8, p. 227 ff.

sa ) ea zone na the Deep will section or the Main Point ©
zt e of Gurley, is homotaxial. with Tullberg’s zone of the
i aptus shales. As we shall see preety his zone a, the

r If (his “lower Graptolite shales”) and Brégger (“ Phyllo-
~ graptus shales,” in Die silurischen Etagen 2 and 3, etc. 1882. p.
asm They found this Phyllograptus shale (8b) between the
_ Ceratopyge limestone (5a 7) and the Megalaspis limestone
eo a). ia ‘ ~
- Holm? obtained species of the Pat eel lias zone, such as
i aie bigsbyi and Phyllograptus angustifolius
- from glauconitic gray Orthoceras limestone (Planilimbata lime-
stone) of Celand and partly based on these his beautiful investi-
gations regarding the morphology of these graptolites.
In France the following species, originally described from the
‘Levis beds, Didymograptus pennatulus, D.
faa toaus, D. bifidus, D. indentus, Tetragrap-
tus serra and TT. quadribrachiatus, have been re-
ported by Barrois? from the graptolite schists of Boutoury
near Cabriéres in the Languedoc. He correlates this schist
with the middle Arenig (Skiddaw) of England, the Quebec beds
of Canada and étage Dd 1 fof Bohemia.
In the succeeding year the same distinguished author an-

be =a? Te oon. ay eas ie a el cd he Se eo - = = pa

_ hounced the discovery of the species described by Hall as
4 Graptolithus richardsoni at La Mouchasse du

. *Skanes Graptoliter I, in Sveriges Geologiska Undersékn. 1882. ser. C,
no. 50.
: *Sveriges Geologiska UndersGkn. 1895. ser. C, no. 150.

Annales de la Société Géologique du Nord. 1892. t. 20, p. 75 ff.

=_

See ga ee ghee a>

re: appears that both the 1 Tetragraptus
graptus bifidus sonea ters sg me be
Cabriéres. ae ite a
From the auriferous shales of Victoria, Aue
has reported the occurrence of such— ge
fossils as Tetragraptus bryonoides
T quadribrachiatus, T. fruticosus,.
graptus typus, Loganograptus loga i
Didymograptus nitidus, to which ree
added Goniograptus thureaui. This list i
the presence of the Tetragraptus zone in Australia.
The preceding brief review of a number of public: ie
which announce the presence of the Tetragraptus: fannel ey ie a
sufficient to demonstrate the vastness of the area which Pes x
once occupied. Prof. Frech? has suggested the probability that .
there existed four grand marine provinces in the Lower Siluric | “%
which were more or less separated from each other, viz the —
Bohemian-Mediterranean, the Baltic, the North Atlantic and
the Pacific-North American basins. The former existence and 4
extension of these provinces is deduced from the comparative
study of the horizontal distribution of the faunas, specially
of their trilobite element. The graptolites however are €x- A
pressly excepted as passing beyond the boundaries of these
basins, and this phenomenon is explained by their pelagic or
abysmal habitat in contrast to the littoral or shallowsea habitat
of the provincial faunas. This necessity of contrasting the
graptolite faunas with the other faunas on account of their
vast geographic distribution, together with the well known
fact of their short vertical range, is a conclusive demonstra- |

* Ann. and mag. nat. hist. 1874. 4th ser. 1:41.
: Geol. surv. Victoria. Prodr. pal. Victoria. Decade 5, 1877. p. 39.
* Lethaea palaeozoica. 1897. 2:88 ff.

»

ee a a Se. ee

| creating ae of ries aoe
a of ae ee of the Beekmantown pm: with

<a — but spread rapidly over wide territories, it is proper to
== ~ conclude that this Tetragraptus fauna, like the succeeding
3 m _ faunas, conquered its territory in a very short time, and that
a we have here, hence, not only homotaxial, but actually syn- |
s ~ chronous beds of both hemispheres before us.
4 The fact mentioned above, that the English and Swedish
2 faunas of this horizon have a greater number of species in
Sy common than they have with the Levis fauna, is, in this connec-
_ _-tion, worthy of special notice, as it proves that a world-wide
and absolute identity of the pelagic graptolite faunas does not
exist. This may indicate that there also existed geographic
4 or regional differences, which, however, did not coincide with the
differences in the distribution of the other fossil organisms, as
has been suggested by Frech (loc. cit. p. 116) in view of the
discrepancies observable in the succession of the two detailed

series of upper Siluric graptolite zones, made out by Tullberg
in Sweden and by Barrande in Bohemia.

: Zone with Didymograptus bifidus and Phyllograptus anna

= 7 Graptolite bed 3 |

f This bed has a thickness of 2 feet, and is separated by 14 feet

of mostly barren limestone beds (bed h) from graptolite bed 2
It has furnished, partly in an excellent state of preservation, the
following forms:

1 Dendrograptus cf. divergens Hall r
2 Dietyonema cf. delicatulum Dawson | r
5 Callograptus salteri Hail r
4 Dichograptus octobrachiatus Hall r

5 Goniograptus thureaui McCoy, var. e

—

in the” case of fe =

sai subdivided se 2 Siluric of ——- Europe. sphiag ae

15 P. anna Hall OS Ts a ae ar
16 P. angustifolius Hall ey ae
17 Nemagraptus sp.
18 Thamnograptus anna Hall
19 Lingula quebecensis Billings.
20 Small indet. brachiopods -
To this zone belong also the beds j, k, L m aed 1
silicious beds, sandy shales and limestones. Bed j ‘be
black shaly partings, Didymograptus biftids
most characteristic form of this zone. The thin grapto !
4 in bed 1] also furnished this species and a few poorly pre
fragments of some of the other forms. _

a $4 ae -
» 2

Graptolite bed 5 Sai

Under this notation have been united the numerous | shi aly
partings between the heavy banks of greenish gray, cringe
hard, silicious rock which is exposed, with a thickness of 52 :
feet, in the quarry at the east end of the continuous section
(stratum o; the shaly partings are denoted on the diagram by
the letter p). Most of these partings are covered to the exclu- wa
sion of other species, with the rhabdosomes of the species — |
Phyllograptus typus, Ph. ilicifolius (large muta-
tion) and Ph. anna. The largest specimens of Phyllo- a
graptus typus occur however in a layer at the base of
graptolite bed 3. The full list of the species observed in the
quarry is: 3
1 Tetragraptus quadribrachiatus Hall

ee ve

2 T. serra Brong.

. ee from the new appearance and abundance of in--
ividuals of Phyllograptus typus, Ph. anna,

«a

Didymograptus bifidus, D. similis and Tham- if

a n ograptus anna. The last four were, together with

‘Tetragraptus fruticosus, described by Hall as

3 occurring in the “Quebec group, 3 miles above the river

Ce Sot eee ee

St Anne.” They pertain, hence, to an association not known —

to him from the Levis region, nor have they, to the writer’s

knowledge, been reported since from the Levis beds, with the
exception of Didymograptus bifidus, which is listed
by Ami (Geol. sury. Can. Rep’t for 1887-88, 53 k) as found

in an excavation near the City hall of Levis and by Gur-
ley as occurring also in another Levis zone identical
with the next succeeding Deep kill zone. Lapworth found
Phyllograptus anna_ associated with some other
species, which are common to this and the Tetragraptus zone,
in the collections submitted to him from the south side of the
St Lawrence river, and termed this the St Anne zone or zone
with Phyllograptus anna. He correctly supposed it to
belong to about the middle of the series of the Levis zones. Dr
Gurley, in compiling the list of the North American graptolites,

_had no collection from the St Anne beds to refer to, and cites

only the forins listed by Hall and Lapworth.

Though the fauna of this zone, as well in the shales of
St Anne des Monts, as in the Deep kill beds, appears rather
limited when compared with that of the preceding zone, it is
notwithstanding of the greatest interest, first stratigraphically,
as it clearly marks a distinct horizon or zone, which is also
discernible in very distant regions, and secondly phylogenet-
ically, as it indicates the approaching suppression of the

—_

od ble in the mame of Se

‘final ptoks of the freely t neh edie er
forms. The species of the “genus is Tetragré
latter reached the acme of its aevelopanine ‘int : ee
zone, are, with the exception of T. quadribrachi ts
cerucifer and alatus, still present, but are 1 ies
only by smaller mutations. The genus Didymogrenteaay
lived into the Trenton period, and with a few | necie
its subgenus Leptograptus even extends into th :
period, appears with two new species, which are restricted to
this zone, and one of which, Didymograptus bifidt 7
is in the Deep kill section the most characteristic species ¢ ) afi
the zone, as; it is extremely common in the beds, exter ds
neither above nor below the zone and is the first of the “ tur ing A
fork” species of the genus, which in Europe are quite | nar on
acteristic of still higher zones. The genus Phyllograptus —
attains in this zone in Ph. typus its greatest size and

variability within the boundary of a species but is also repre- _
sented by the diminutive Ph. anna, which also extends
into the next zone and foreshadows or closes the life history
of this peculiar genus. Finally there appears in this zone the
first of the coenograptids, which attain their full development —
not before the middle part of the Champlainic or Lower Siluric.

Lapworth’ reports a similar association, characterized by
Didymograptus bifidus, D. extensus, Phyllo-
graptus typus, Tetragraptus bryonoides and
T. quadribrachiatus from the “Ballantrae rocks” in
Ayrshire, south Scotland. Miss Elles lists Did Ymograptus
bifidus as occurring in the middle and upper Skiddaw

—

Géok mag. 1889. 3d ser. 6:22,

dt oe te ots he ds as

r Deep ill zone, ene. ae species, ae poe
= anna, are according to Miss Elles found there in

i ted (loc. cit. p. 529): “Tetragraptus serra (Brong)
. and other forms are also found associated with the fauna which
in Sweden characterizes the zone of Phyllograptus of.
# Rigs us and occur on the same slab as the earliest tuning fork

subzone (corresponding to the upper Arenig) with which we have
4 a to correlate the present Deep kill zone or the St Anne beds of Canada.

Didymograptus gf. bifi dus forms, according to Tull-
berg, the highest part of the lower Graptolite shale and over-
lies the Orthoceras limestone (limestone with Megalaspis
_ planilimbata and Megalaspis limbata). But,
as this zone is also reported to contain Climacograptus and
: Cryptograptus, which here do not appear till the next zone,
this Scanian and the Deep kill zone can not be exactly
parallelized; and it is to be assumed that the former holds
a position intermediate between this and the next Deep kill
zone, and that the St Anne beds are homotaxial with the Megalaspis
limestone itself.

In Bohemia a form from étage D di y has been identified with
Didymograptus bifidus by Dr Perner;! and in France,
as noted before, Didymograptus bifidus and Rou-

vVilligraptus richardsoni, two species of the St Anne
7 beds, have been reported from the graptolite shales of Cabriéres.
Finally, the zone with Didymograptus bifidus was
recognized by T. S. Hall? as a separate horizon in the aurif-
erous shales of Victoria in Australia, where it also overlies
the Tetragraptus zone. It appears that in Australia and New

* Etudes sur les Graptolites de Bohéme. 2iéme partie. 1895. p. 23.
* Austr. ass’n ady. sci. 1898. 5:374.

be bifidus, specially Phyllograptus typus _

iddle Skiddaw slates. In regard to this association it is”

_ Didymograpti.” This association forms the upper Tetragraptus

In Scania the zone with Phyllograptus cf. typus and ©

following fauna.

a ey Phylibgeipt es angustiolins 5 i pay
2 Ph. sp. nov. doc

3 Diplograptus dentatus Brong.

4 Retiograptus tentaculatus Hall

5 Of. Trigonograptus ensiformis Hall (fragments)
A larger fauna was obtained from

Graptolite bed 7 ages
This bed consists of soft, black shale, the bedding p | nes: )
which are profusely covered with specimens. It furnish

1 Dendrograptus sp. nov.
Dictyonema sp. nov.
D. sp. nov.

to

ee

D. (Desmograptus) cancellatum Hopk.
D. (D.) sp. nov.
Callograptus diffusus Hall
C. sp. nov.
8 Ptilograptus plumosus Hall
9 Loganograptus logani Hall
10 Dichograptus octobrachiatus Hall (hexad type) ,
11 Didymograptus (Isograptus) gibberulus Nich. var. nanus, ‘i 7
var. nov. c

1 0 Ol

12 D. sp. nov. rr
13 Leptograptus sp. nov. bi.
14 Nemagraptus sp. indet. c
15 Diplograptus dentatus Brong. (=D. pristiniformis Hall) cee
16 D. inutilis Hall r

ee
Ogre eae apechen Hall
igonograptus ensiformis Hall

in acograptus Sp. nov.

. from talcose mud pebbles. This nas Br ceed.

1 Dichograptus sp. (branches) :

2 Phyllograptus anna H all |

3 Diplograptus dentatus Hall : ce
| “4 D.z sp. nov. | B
a _ The aspect of the faunas of these two graptolite beds, which
s Pia belong to one zone, is totally different from that of the
two preceding zones. Not only are all species new, with the ex-
¥ ception of Loganograptus logani, Dichograptus
[eoeetobrachiatus, Phyllograptus angustifol-
ius, Ph. anna and Lingula quebecensis, and
the prevailing genera different, but even the subclass of the
Axonolipa, which hitherto alone held the field, has almost en-
tirely been replaced by the family Diplograptidae of the Axono-
phora. The latter are represented by the genera Diplograptus,
Climacograptus, Glossograptus, Cryptograptus, Trigonograptus,
and Retiograptus.

A peculiar feature of this fauna is the sudden outburst of
the Dendroidea with a Dendrograptus, four species, in numer-
ous individuals, of Dictyonema (two of these of the rare sub-
genus Desmograptus), two Callograptus and a Ptilograptus.

. This subclass however, though reaching its acme already

4 Cambric beds, reappears, as is well known, with great force in
; the Niagaran and extends even into the Hamilton formation.
As only the species of Callograptus and of Ptilograptus, one
of each genus, are recorded from the Canadian exposure of this
zone, the greater number of species and the profusion of speci-

he oe zones shows
that this is hardly the case, for in the Skiddaw b ae as, on as
the same two zones have been found in direct suce a
true, there may exist an intermediate, transitional zone, ¢
ing a more balanced mixture of the two faunas, such as

found in Scania (see above, p. 569).

All the species of this fauna, described by Hall, ry
him simply as coming from the Quebec group of Point a
In each description, however, the association is recorded in y ec )
the form was found, and from these records it becomes evident

re

that the separate existence of this peculiar assemblage of s De cles

at Point Levis was well known to that illustrious observe er.
Lapworth (loc. cit.) found no material from this zone in cage : a
lections submitted to him, and therefore does not mention Ss
locate this horizon in his series of graptolite zones. es er

Dr Gurley (loc. cit. p. 302) states that besides the fauna of the 4
Main Point Levis zone he had before him a smaller collection of <a
Point Levis shales, from a locality 14 miles north of the east ©
railway station at Levis, which has a strikingly different fauna; —
adding: “It was remarkable not so much for the species present
(though the Diplograpsidae seem highly characteristic) as for
those absent.” His Ordovician table of graptolites (loc. cit.,
p. 296 ff) proves that the third Deep kill fauna is identical with —
this second Point Levis fauna. Gurley calls the latter simply
the “ Point Leris fauna,” and, together with two similar associa-
tions, from the Pijion range at Summit Ney., and from Arkansas,
refers it to the upper Calciferous zones.

In England the zone with Diplograptus dentatus,
Cryptograptus antennarius and Trigono-
graptus ensiformis is well developed in the Ellergil

hE

corresponding Point Levis zone and Phyllograptus

_ this zone.

es the Llanvirn beds of Wales; and by Miss Elles with Tuil-
_ berg’s zones n), zone of Glossograptus and 0), zone of Didymo-
graptus g emtnus, which form the basal part of the middle
3 Be cnitolite shales or of the Dicellograptusskiffer of Scania. These
zones also contain the genera Diplograptus, Climacograptus,
oe ~Glossograptus and Cryptograptus. The latter zone has again
q _ been subdivided into three subzones, the lowest of which
(still contains Didymograptus bifidus. This
% would suggest that the presence of the above cited species of
the Phyllograptus anna zone in the zone with Dip-
| lo graptus dentatus in America may eventually allow
the recognition of subzones in the latter.
- It will be noticed that in England this zone is plaved above
: - the Arenig formation, and that the corresponding zone in Scania
4 is united with the middle graptolite shales, that, hence, impor-
| tant formational boundaries separate, in Europe, this and the
| preceding zone. This fact,in connection with the decided change
in the character of the genera, which are those of the Middle
: _ and Upper Champlainic or Lower Siluric, may with our advanc-
| ing knowledge of the graptolite facies of the Champlainic lead
to the correlation of this zone with some part of tne Chazy
formation. This supposition seems to be well supported by a
statement of Mr Walcott (see Gurley, loc. cit. p. 304), that “in
Nevada Didymograptus bifidus occurs in strata cer-
tainly supra-Calciferous and probably of Chazy horizon.”

*Geol. mag. 1894. 14th ser. 1: 127.

h err aaa: Pp hi y Ho Ce) aa ra “ it us anna Sand
ograptus angustifo lius are not reported by a
les from | these beds. Marr,! however, also cites the lat- pe
ies. As Dr Gurley has also found Did. bifidus _

anna in association with these Diplograptidae in Arkansas, _
ty as is apparent that these species rise in various regions into

Fh fs

« S78,
ts,

=

—
Sd
be
Te
‘a
7

The Ellergill beds are correlated a Lapworth, Marr and Elles —

4 ¥

p.* Db Zone with iptrabibeh |
Bere graptus anna .
| a Zone with iets i!

and Scandinavia, all three zones have been ubecegen in a
succession. In Canada, zone a is known from sever 1 reg
the most important being the Levis and St John resionts a
typical fauna of zone b has become known from the be :
the St Anne river in Canada, and zone ¢ is again present in t he
Levis beds. The succession of these zones has thus far not. bec 1
reported as observable in any of these Canadian regions. Ay ae 4 t

The stratigraphy of the Deep kill section demonstrates that the
Main Point Levis beds or those of the Tetragraptus zone are ne
lowest of the series; that they are followed by the St Anne beds or va
those of the zone with D idymograp tus bifidus etc,,and
that the Point Levis beds, containing the zone with D iplograp- oe
tus dentatus etce., overlie either directly the St Anne zone or a
are separated from it by only an intermediate transitional zone. :

As the Levis beds have been demonstrated to belong to the
Beekmantown or Calciferous formation, the two lower of the
zones certainly represent part of the graptolite facies of that
formation, while the third zone may either belong to this or to —
the Chazy formation. =

In using the results of a former investigation by the writer
of the shales in the vicinity of Albany (N. Y. state mus. Bul. 42)
the zones recorded in the first column of the following correla-
tion table of the Champlainie or Lower Siluric graptolite shales
can be claimed to have been discerned in this region.

SE Se a ee
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a es an — ‘This remarkably pretty

“graptus eyecare h

- field, Sandhurst, Victoria, RS: ieee it. was
by McCoy. It is there, as in the Levis and Deep kill b 2d
associated with the species characteristic of the Tetr:
zone. Dr Ami figured a remarkably large and perfect spec
and added the description of the central disk which ex
a peculiarly alate manner along the branches. 3
In the Deep kill section numerous hydrosomes
species have been found, not only in the Tetragraptus zone, b
also in the beds of the overlying zone with Didym ogra
tus bifidus and Phyllograptus anna. The =e
terial from the former zone proved to be of special interest for
the study of the ontogeny of the species, for it contained a com-—
plete series of finely preserved growth stages from the sicula — a
onward to the mature colony. These stages allow the elucida-
tion of some points in the ontogeny and morphology of the ‘aetlh ~ 3a
tiramose dichograptids which were hitherto not well under-

stood; and they have therefore been made the subject of this pe?
notice. : rs bg

A restricted number of characteristic stages has been figured.
The outlines of the figures have, with one exception, been drawn
with the camera lucida and reduced to their present size.

Sicula. The sicula itself is rather short and stout, as those
of many other dichograptids; it can, therefore, when alone, be
hardly distinguished from the siculae of several other species
occurring in the same beds.

*Can. rec. sci. 1888-89. 3:422, 502.

* Ann. and mag. nat. hist. 1876. p. 128; Geol. Sur. Victoria. Prodr. pal.
Victoria. Decade 5. 1877. p. 39.

‘reaui McCoy. Fig. 2 Idem. Sic-

var. postre- Les Rom Suneens
wo i fomus,... Sieula, side); an ranches Fig. 3 Idem. Same
- and first two of first and second or- P 2 .
thecae (fun- der. x3%4 | from sicularside. x31
icle). x3

4 2, which, growing across the “antisicular” side of the sicula,

a >

diverges to the opposite side under exactly the same angle as

theca 1. In older colonies the thick, straight, uninterrupted
cross bar between the principal branches has been termed, in
other multiramose dichograptids, the “funicle” by Hall and
succeeding authors on graptolites. As the somewhat larger
colonies usually settle on their broader surfaces, the sicula is
brought into a vertical position, and hence often fails of observa-
tion in the fossilized state, as in fig. 4, where the central thick-
ening indicates its location.

Each of these primary thecae produces in its turn (fig. 3), in
a like position and manner as the sicula did, a new theca, which
also, after a short adherence to the mother theca, turns aside
at the same angle as does theca 1 and, like the latter, sends a
new theca, corresponding to theca 2, to the opposite side. The
bifurcation near the aperture of the sicula of the first two
thecae is hence repeated at the aperture of each of the latter,
and four secondary thecae result. These four thecae form the
four “ primary branches ” of other authors. Each of these pro-
duces a new bifurcation (fig. 5 and 6) by the same process
of twice repeated gemmation in two succeeding thecae, and the

_-

a horizontal position in the drawing (fig. 7, 8), the four t rheea

of these eight tertiary ones, which lie on the side of the vert
axis (A-B in fig. 8), produce thecae which do not divers
their mother thecae, but retain the direction of the latte
leads to a serial arrangement of the thecae and to the &
late RESELRGP mt % ver authors. The other as tertngy

Fig. 7 Idem. Next growth
stage. Differentiation of ar-
rangement of thecae has com-
menced. abranches with seri-
ally arranged thecae; at b dich-
otomy continuing. Xx2l¢ Fig. 8 Idem. A further advanced growth s

which shows more distinctly the differentiation of t

tertiary branches (IIL) and the composition of the tent

jatagea we stems of thecae (see thecal apertures in upper
ft quarter). x2.

bifurcation. They become thus component parts of the prinei-
pal stems of the mature colonies.

Of the eight tertiary branches Gaaeeey III in fig. 8) resulting
from these bifurcations, those subparallel to the funicle become
denticulate, while the others bifurcate again.

oO

7

OQ
/
i?
lL?
f

Ss

lh

1

|

ary \
Fig. 10 Idem. Stage where dichotomous
of branches seen from thecal side. “2232 °° Strange themselves serially. Nat. ize
branches, six on each stem and none of the many hydrosomes ob-
tained at the Deep kill have a greater number of branches than
six. As the ultimate branches of the stems are both denticulate,
dichotomous branching appears to have ceased, and 24 seems to
be the maximum number produced by these colonies. Dr Ami,
however, figures a very large specimen, which, when complete,
would have had about 80 branches. Specimens in the writer’s
hands attain about three fourths of the size of that referred to,
without bearing more than 24 branches; also the smaller speci-
men figured by Dr Ami possesses a greater number of branches
than colonies of like size in the Deep kill collection. These facts
seem to indicate that the latter material contains a variety
which, in the process of reduction of the number of branches,
observable throughout the Dichograptidae, has advanced a de-

cided step beyond the original Goniograptus thureaui,

H

Fig. 11 Idem. Mature hydrosome. Shows can veskehsted, eI
branches (4), in this variety. Nat. size a7

end of the Goniograptidae, as far as the genus is wl , an
might be designated as Goniograptus thureaui ¥ r.
postremus. ee
The important ontogenetic and morphogenic facts of whid i. a
this series of growth stages permits a statement are:
1 Phe “funicle” of Goniograptus consists of two thecae. The’
equal length of the two parts of the funicle between the
sicula and the first dichotomy and of the primary branches —
in the other multiramose dichograptids indicates that the
funicle is in all these constructed of two thecae.” With ad-—
vancing growth of the colony, the two thecae of the funicle,
like those of the principal stems, become greatly thickened
and assume the form of cylindric stems, thus more or less
losing indications of their former thecal nature (fig. 10 and
11). The statement, found from Hall's work onward in nearly
all descriptions of the colonies of these multiramose dichograp-

. a theca on each side of the sicula in fe funicle of Troch-
é yera ptus diffusus. Concerning the structure of the
a? funicle in general that keen observer states:?

On these grounds, and in Pome wbeuatian of the many- -branched

_ Dichograptidae being embedded in shale, and therefore showing
the thecae of the central part of the polypary only in very excep-
3 3 tional favorable cases, and as these thecae are analogous to
___ those in Didymograptus and other forms which are better ex-
_ posed, I draw the conclusion that the funicle in many cases, if
not always, was furnished with thecae.
4 - This conclusion is fully verified as to Goniograptus and Coen-
ograptus (fig. 13) by the writer’s material. It becomes appar-
ent from these observations that the funicle does not differ in
structure from any other part of the stem; and probably in all
Dichograptidae consisted of two thecae.

2 The four principal stems of Goniograptus are composed of
thecae, each internode between two bifurcations consisting of one
theca. For this reason all these internodes are of uniform
length, and, because the angle of divergence of the budding
‘thecae is constant throughout, the angles of bifurcation are all
alike.

The next related genus, Clonograptus, which develops the
greatest number of branches and is most irregular in the
extent of its branching, has been considered, on account
of these characters and its earlier appearance, the progeni-
tor of a part of the multiramose dichograptids. It is a well
known character of this genus that the internodes between
the bifurcations not only grow to extreme length, but also

TS A ee ne eee

*Geol. mag. 1895. 4th ser. 2:484.

Af
“wn

;
g

‘ Fig. 12 Clonograptus (Goniograptus) sp. nov. Possesses long ‘stem 1 inte:
consisting of but one theca. x21

stems of these forms, in conformity with Hall’s font amen al
views, have been currently considered as entirely ae ee
or free from thecae, they have not been investigated as to their
structure, and conclusive data on the number of thecae in each
internode are not to be obtained in the literature. Hall’s poli

tion! was this:

Neither the central portion, nor any of its subdivisions
becomes celluliferous; and these parts are not termed stipes
or branches, according to the views I have entertained. It is
only beyond the last subdivisions of this part of the body, as in
G. logani, that the celluliferous parts, or the true stipes,
commence.

Miss Elles? states that she has observed thecae on stipes of
every order in Clonograptus flexilis. Of special in-

terest in this connection appear to be the description and illus-
Oe
Can. org. rem. Decade 2. 1865. p. 20.

? Quar. jour. geol. soc. 1898. 54: 473.

ser and distinctly fiured as Faveethi of several theese?
: ee oPere this species ee ests lower Siluric species of

nches are equally short, a tendency toward a concentration
f the dichotomous branching in the central part of the colony
F P. costes apparent.
- Ss _ The genotype of Dichograptus, D. oc tobrachiatus,
and that of Loganograptus, L. lo gani, are found associated
3 with Goniograptus in the Deep kill es and occur in younger
x Specimens, which indicate that these genera also conform to
4 Re. the composition of the internodes of one theca each.
. --'The denticulate nature of the branches of the first and follow-
ing order in Temnograptus was already known to Hall (Gr.
- milesi Hall) and has been recognized in its related genera
(Holograptus, etc.). ;
Holm has described a coenograptid (Pterograptus
ele gans),?with a distinct thecal structure in the two principal
: stems, and the writer figures (fig.
-_-13) a young specimen of Coeno-
; Seapius. gracilis. itself,
: which distinctly shows the thecal Ws
| structure of these stems. :
It becomes therefore probable
that all parts of the hydrosome of
the Dichograptidae, including fun- iy 13 coenograptus gracilis Hall.
icle and principal stems, consist of of funiele and principal stems of thecae.
Normanskill shale of Mt Moreno. x4
thecae; with the exception of the
nema, which carries the sicula, and of the central disk.
3 The growth stages of Goniograptus indicate that the bifur-
cations of the branches throughout the hydrosome take place in

*N. Y. aead. sci. Trans. 1895. - p. 295.
2Ofversigt af K. Vet. Ak. Férhandl. 1881. no. 4, p. 77.

=_

tus, obtained in the Deep kill collection it ce lec
the dichotomous branching of these ‘genera “€ nfo :
same law. The hydrosome of a new species of. Br ryO% 5
common in the Tetragraptus beds, possesses the same a
branching. *

Holm! has demonstrated that in Didymograptus, Ts
and Phyllograptus the same mode of branching rite

As to the nature of the branching which has we
“ monopodial ” or “lateral,” and which is characterized b
continued growth of the original branch in the same dir e
after division, I have been unable as yet to obtain any con-—
clusive facts. The genera which show this mode of branchir ug “ai og
most typically, are Schizograptus, Trochograptus, Holograptus | i 3
and Rouvilligraptus. The fact, however, that both dichotom- ;
ous and monopodial branching coexist in the hydrosomes oh
these genera, seems to indicate, that there can be no funda-_
mental difference between them. Observations on Coenograp-
tus (fig. 13) indicate the correctness of the suggestion of Wiman? =
that this mode of branching is produced by the greater strength | ee
which is attained by the mother theca before it produces the
daughter theca, and which enables the former to retain its
viginal direction while it compels the latter to a change of

direction.
4 There must have existed physiologic and morphologic
differences between the zooids of the biserially arranged

*Sveriges Geologiska Undersékn. Afhandl, och uppsatser. 1895. ser, C,
no. 150.
* Geol. inst. Upsala. Bul. 1895. no. 4, v. 2, pt 2, p. 34.

ns sand feet of ae feocles ix grow in the iecetioh
1e ‘mother theca. It is further evident that the essentially

er ... ye function of nutrition while those of the stems
=e; etc.) served this function only in the early stages of the
eolony, and later on, when they became thickened by chitinous
Waeiasita into cylindric stems (compare fig. 10, 11 and Hall’s
ae of TOS ee ae rigidus), assumed as their
principal or sole function the supporting of the branches. It
_is partly on account of this secondary adaptation to the latter
function that the thecal nature of the stems has failed, till
lately, to be recognized in the majority of the dichograptids.
a This difference in function is, to some extent, also expressed
a _ in the morphologic differences between the stem thecae which
; we here call stolonal thecae,! and the branch thecae which may
: be termed brachial thecae. If one compares the extreme
4 thecae of the branches of Goniograptus with those form-
a ing the stems (fig. 10, 14), one can not fail to notice that they
differ. The latter, stolonal thecae, are more cylindric, very
2 slightly widening toward the aperture and without any sub-
mucronate apertural processes; they, therefore, usually fail to
appear as “ denticulations.” Their apertures are small, circular
openings (fig. 3,4, 5). The fully developed distant thecae in the .
branches widen more abruptly toward the aperture, have wider
apertures and submucronate processes on the outer apertural
Margins. These differences can not be due to different degrees
of compression in consequence of different thickness of
periderm, or be caused solely by the superposition of the thecae
on the branches.

*The first theca of each ‘‘ denticulate”’ branch is to be considered ag

& stolonal theca on account of its assuming a direction different from
that of the mother theca.

» id ' fa 7
‘<- iy 9 ce
tie Pe tie 4 ae

t, tol
4 rane cate te Ba

later thickening and aE: 3
cient to indicate an important difference in t the he zooids 1
occupied the thecae. aa
5 The stolonal thecae are more similar in Baa anda
to the sicula of the colony than the brachial thecae. They w
a similar degree and possess the same simple apertural m
In general, it may be said that all the thecae of a hydr
conform to some extent to the sicula of that hydeonome, forr
with long, slender sicula, having similar thecae and s
wider, shorter sicula, as numerous Tetragrapti anal See é
mograpti, having correspondingly shorter. thecae; but es rh
Same time, the sicula of each colony is still relatively longer hie: 3
narrower than the average or extreme brachial theca. = = a
A comparison of the form of the thecae of the younger dicho- e.
graptid genera, as of Dichograptus, Tetragraptus and Didymo- eat
graptus, with that of the older and presumably also phylogene- —
tically preceding genera, Bryograptus and Clonograptus, shows Pa
that, in general, the older genera have the more tubular, simpler
thecae with less protracted apertural margins. It is, hence,
apparent that the stolonal thecae and the sicula represent the
older type of thecal form. a
6 The growth stages of the hydrosomes of G oniograptus
thureaui prove further that also within each branch only
siculoid thecae are at first produced (fig. 9, 10, 14). In fig. 14
the basal and distal parts of a branch of Goniograptus
have been still further enlarged to show their differences more
distinctly. The earlier thecae a, are tubular, lie subparallel
to the axis of the branch (the angle between the axis and their
outer margin is only 7°), overlap not more than one fourth of
their length, have a straight aperture without marginal process,

a. from the sicula through the stolo-
nal and early brachial thecae to

e apertures and a genre
etme outer eee margin.

of ae colony of Goniograptus,

the distal brachial thecae, form an

mee oteercactic series, which furnishes , oo rcmus abransn: b promimal thee

_ a clear and interesting example of

enlarged; c distal thecae enlarged.

“localized stages of development ”, the existence of which has
been demonstrated and their character elucidated by R. T. Jack-
son. In this remarkable publication it is stated (p. 90):

In organisms that grow by a serial repetition of parts, it is
found that there is often an ontogenesis of such parts, which
is more or less clearly parallel to the ontogenesis of the organ- >
ism as a whole. In the ontogeny of such localized parts in a
mature individual, we find stages in the development during
the growth of the said part which repeat the characters seen in
a similar part in the young individual. To state it briefly for
the moment, such localized stages have been observed in the
leaves of plants, in branches or suckers of plants, in the bud-
ding of some lower animals, as Hydra and Galaxea, in the plates
of crinoids and Echini, in external ornamentation in mollusks,
and in the septa of cephalopods. |

From the examples cited those of Hydra and Galaxea are the
most pertinent to our inquiry. In regard to them Prof. Jackson
makes the following note (p. 141):

In animals which produce asexually by budding, as Hydrozoa
and Actinozoa, it seems that the bud may be considered a local-
ized stage. The bud has not the stages seen in early embryonic
development from the egg, but repeats in general the later
stages seen in such ontogeny. A bud is not a new individual
in the full sense of the word, but is an outgrowth from an older
individual by a special localized development.

* Bost. soc. nat. hist. Mem. 1899. v.5, no. 4.

_

Fig 15 Tetragraptus desires to illustrate these ontogenetic

fruticosus Hall. Branch

which shows
change of thecae.

progressive
X235

lar theeae, with oan posi ;
rangement, smaller deviation f
rection of the axis of the
straight, not mucronate ap
wise, the whole colony was d
colonies composed of such thecae, |
still retained in its oldest parts. The Car
bric species of Bryograptus and C lo 10g p
tus exhibit well these types of he
rangement and structure. In ie
Tetragraptus, Didymograptus and-
graptus, where, within the Dichogaiall eet ay
the thecae have advanced farthest beyond — ;
their original form, the process of ontoge- a
netic acceleration has also gone farthest in q
effacing all vestiges of the original thecal _
form, ase.g.in Didymograptus (Iso0- |
graptus) gibberulus, where no sicoi- .
dal thecae are preserved. In others, how- |
ever, as a study of Hall’s excellent
figures of the various species of Didy-
mograptus will show, the gradual
change from tubular to more gibbous,
more closely arranged and more erect Se
thecae can clearly be traced. The writer |

changes in the stages and arrangement of

eRe CMe

‘

i gees as. taraxacum (ig. 19). ‘The |

Fig. 1€ Tetragraptus tar- —

- axacum sp. nov. Shows

change from narrow Fig.17 Didymograptus (Leptograptus) sp. nov. Pos-

_ to wide thecae. x31¢ sesses short proximal and = distal thecae. x3

‘That the direct opposite pattern to this compact structure

represented by Tetragraptus and Isograptus, namely the ex-

tremely slender and graceful colonies of Leptograptus with their
long filiform thecae, are likewise derived from a form having the
Bryograptus type of thecal structure, is shown by the colony
of a new species of Leptograptus from the Deep kill beds, which

is represented in fig. 17. Here we have in contrast to the onto-

genetic changes noted before, tubular proximal thecae,. suc-
ceeded, as the branches lengthen, by extremely thin and long
distal thecae which hardly deviate from the direction of the axis
of the branch. The outgrowth of such extremely different, mor-

_phologically contrasted branches as those of Tetragraptus

fruticosus, or T. taraxacum and of this Lepto-
graptus from the identical type of proximal brachial thecae
is certainly a strong argument for the propriety of viewing the

changes within the branches as being of ontogenetic nature,

and of corresponding phylogenetic importance.
Furthermore, the fact that the thecae within the same colony

show a gradation from phylogenetically older to younger forms,

and-therefore, analogous to the organ of a growing individual,
pass through ancestral stages, as, e. g., do the septa of a cephalo-
pod shell, demonstrates how closely the zooids of this colony
were united into one organism, and that practically they were

=—

morphologically approaches closely to t ‘the
individual, e. g. the Siphonophora. | ve tant
of the graptolite colonies indicate that they also pe ‘to:
considerable degree of the character of a morp holc logic
vidual. This is specially suggested by the shservatio 0:
several of the composite dichograptid colonies, as i
by the minute stages of Tetragraptus and Phylliogt oes
(fig. 18, 19), even in the earliest stages developed, | me
rapid budding from the ex- _

Bri fe -
Ui: tremely small immature tl
InP W cae (thecae are here mea

Fig. 18 Tetragraptus Fig. 19 Phyllo- tO include or represent t

ig. 19
bigsbyi Hall. mute grapteeihc
xrow HA k Mia, Sioulare and all. Very zooids, which are not oo
-antisicular views. x3}¢ young cont stage.

servable), the fundamental — “4
lines of the mature structure. This was possible because
the buds are produced near the proximal ends of the aa
mother thecae. Only afterward the thecae grew to ma- —
ture size. This premature inauguration of the process” a 3
of gemmation in individuals which have attained only a
small fraction of their mature size, while reproduction in
ihe animal kingdom takes place normally only in adult speci-
mens, and the subsequent expansion of the whole stage, demon-
strate that the early stages of these colonies did not grow by
mere addition of buds, but also as entities. In the latter
process, however, the thecae (zooids) appear entirely devoid of
individuality and only as the subordinate parts of a whole grow-
ing body, which is then, certainly, to be regarded as a morpho-
logic individual in so far as it grows as a unit or individual.
The same uniform growth of the whole young colony took place
also in Goniograptus, as the comparisons of the dimensions of

Be pesiogic individuality of the colony. Some of these are the

ae ae of a common float or pneumatophor, observed in sey-
; a eral groups, and the geometric arrangement of the branches,

a ‘which becomes progressively more rigid, and which served to

_ aay =e"

maintain the equilibrium and to give to the greatest number of.
apis the most advantageous position. ba
- If the graptolites so closely approached the morphologic ae

of an individual, it may be expected that, like an individual, the

whole colony had its ontogeny and repassed ancestral stages.
To these stages, as a glance at the regularly changing features.
of the growing colonies of Goniograptus will show, may be

‘properly applied the terminology introduced by Hyatt for the

ontogenetic stages of an individual.

The embryonic stage is clearly present in the initial part of
the sicula, which, as Wiman has demonstrated, is differ-
entiated from the distal part of the sicula by the nature
of the periderm, which is thin, pellucid and possesses no growth
lines. Holm! asserts his belief that this initial, more pointed
end of the sicula “ corresponds to the original chitinous cover-
ing of the free zooid germ or embryo.” This initial part holds:
a position similar to the protoconch of the cephalopod shell.
The nepionic or infantile stage is represented by the stages
(fig. 1-6) in which the successive dichotomous divisions produce
the stems. It begins with the formation of the apertural part of
the sicula. The neanic or adolescent stage of the colony begins
with the formation of the branches with serial arrangement of
thecae and ends, in the Goniograptus material from the
Deep kill, with the production of six such branches on each of
the four stems. After this, in the ephebic or mature stage, the
branches continue to grow out to full length. Distinctive

*Geol. mag. 1895. 2d ser. 32:435.

=_

Diaynwerres tee bitidue:t
As they serve more to verify the alaaeaationi
graptus thureaui than to bring out news
description has been deemed basicity in ~~ pre
publication. ae Pe us

ee DESCRIPTION OF A
a FOSSIL ALGA FROM THE CHEMUNG OF NEW YORK
| WITH REMARKS ON THE GENUS
HALISERITES Sternberg

BY DAVID WHITE
Plates 3, 4

Though scores of fossil bodies from the Devonic and Siluric
in both Europe and America have been described and published
as seaweeds, few of them are now generally regarded as”
vegetable, the greater number having proved to be of animal
or mechanical origin. Even among those survivors whose out-
lines and superficial aspect. would seem at once to proclaim
their unity with this great class of lower cryptogams, a very

small number only are wholly free from the suspicion that they
should be relegated to the sponges or the graptolites, or
accounted for as the burrows of some other organisms. The
admitted identity of the small remainder of Paleozoic thallo-
phytes is in most cases based on the internal organization of
such fragments as are sofossilized as to reveal their microscopic
structure, rather than on their form and external characters.

The unsettled and somewhat chaotic status of the supposed
Paleozoic algae can not be due to any lack of seaweeds during
Devonic or Siluric time. Plant life of this class must have been
and undoubtedly was in great abundance. The apparent rarity
of unquestioned Paleozoic algae is due in the first place to the
absence of hard parts in most seaweeds and the consequent
failure, except in extremely rare instances', of preservation of
any portion of the plant, specially of fragments showing the
essential primary diagnostic details relating to anatomy or re-
production. Another partial explanation lies in the remarkable
Similarities in form and habit between many algae and certain
contemporaneous low animal types, specially among the sponges

* Chiefly in the coralline types.

, . 7 a.) eo
jatter. |

ficiently complete to show at once the for m 0: :
while at the same time affording some hint wr io’
structure. The material described below includes two 0 D1
extremely rare and important examples. ei
The principal specimens described in this paper are € ox] posed —
on a slab from the Chemung strata at East Windso 3 ,
co., and presented to the state museum by E. B. He i all ¢ f We
ville N. Y. The slab is of greenish gray micaceous | =a
and is rectangular, being about 73 cm long, 32 em wide and 1
thick. The lower surface (with reference to its ori |
sition) reveals the ferruginated remains of two or more : es A
ing and beautifully displayed algoid fronds, one of which 3) y a 7
appears to be nearly complete. The lower end of the slab also
reveals portions of four segments that may either belong —
to a single frond or to the same tuft. Evidence of current —
action and rapid deposition of sand is seen both in the dragging
of the large frond, and in the burial of the basal and lower por- x:
tions of all the fronds before the more distant segments were
covered by the sand. Accordingly we see the fragments in
another of the fronds traversing the entire thickness of the —
slab, while the basis of the segments is not represented on this
slab, having been contained in the underlying rock. All the
segments lying at the plane of cleavage of this surface of the
slab show effects of current dragging in a direction slightly
oblique to the longer diameter of the slab. In the fine fragment
shown on pl. 3, the deformation is more pronounced, while in
both the peripheral and the thicker portions the lamina show

+ os a
%

the outlines | s well as a partial obliteration of the
pephemagee * ae A : a

onaceou fatter which is now oe he es oF ie. re-
L by” oxids of iron. The normal aspect and habit of the
nts is rather pare Be ig eas by the fran on pl. 4 (fig. 1)

Beis. The latter features are shown to better advantage
in the fragments of still another frond preserved on the oppo-
site (upper) surface of the same slab.
2 = In all the fragments the depth of the impression, the aS
3 of Bice at the margin, the position and outlines of the
4 branchlets in the compressed form and the amount of carbon- ©
r 3 aceous matter show that the substance of the fronds was thick
_ and fleshy. At the same time a close examination reveals the
presence of a narrow median strand generally appearing in
low relief but sometimes as depressed. The fleshy character,
the median axis and the form of division or habit of the frond
appear to distinguish the plant in hand both generically and
specifically from all other described forms of supposed Paleozoic
algae. In this instance, as in so many other Paleozoic types,
- including many genera of ferns, in which the organs of repro-
duction are unknown, the generic classification necessary for
the proper recognition and paleontologic treatment of the
fossils is wholly artificial!
The plant from East Windsor may be described as follows:

£ THAMNOCLADUS gen. nov. a

Fronds ramose, alternately dichotomous from the base upward,
more or less elongated; lamina fleshy, linear, convex or subcy-
lindric, tapering graduaily, and traversed by a central axis or
strand.

+The name preposed for this plant applies to the intricate copselike
growth of the fronds and carefully avoids all implication of relationship to

any particular family of living algae,

=—

be nl |. ed
~ 7A yo ad ‘
ih 5 a: pe LATS - .
* *; a jee ‘ 7
‘ pe pny a = “ .
4 Sp : Renee & ‘

RSSy eS

fi
yd ance
the penis parallel, forking at a parr i id gle
slightly recurved above each bifurcation, produotey a a gi
subflexuous form; central axis or strand slender, —

mii: re Fe

nearly so in the impressions, generally parallel to the bi rder
forking at a narrow angle a little below each aichotouiga at eS
frond, tapering gradually upward, generally discernible through- _
out the greater portion of the flattened or macerated imp or Ss i
though often obscure in the basal portions or terete fragmer ts ie = ae
One of the more important as well as conspicuous chara ie
of Thamnocladus clarkei is its mode of par ray
regularity and relative symmetry which, combined with tl ne
slightly divaricate attitude of the branchlets, results in a phe ee
ful flexuosity. The details of this habit which may be noted betel a
the slender branches on the right on pl. 3 and pl. 4,fig. 1, are still —
more clearly seen in two isolated branches on a small slab! front.
Meshoppen Pa.,shown on pl. 4, fig. 2. The more delicate segment a
in the latter beautifully illustrates the characteristic bifurca-
tion and the gradual narrowing of the lamina with each succes-
sive subdivision. The width of the ultimate lobes is nearly the
same, about Imm, in all the examples. The Meshoppen speci-
mens also indicate rapid sedimentation, since the lower portion
of the fragment on the left completely traverses the slab, over
lem thick, in an oblique direction. Its downward continuation
was in lower strata. The central strand, while slightly clearer
in the better preserved Meshoppen fragments is in precise agree-
ment with the fronds from East Windsor.
The substance of the lamina in all the specimens has been re-
duced to a compressed carbonaceous residue which is mostly re- — |

*No, 25072 of the Lacoe collection, United States national museum.

nents this ne is obscurely marked in ee specially
the axis, by irregular longitudinal lines or striae; but neither.
se nor the rather indefinite strand seem to present a distinctly
ae vascular aspect. The characters of the residue more strongly
) _ suggest the modified or pseudocompound structure of the more
—_comptcately organized algae, as in the stems of certain of the
_ Phaeophyceae, rather than the vascular bundles or veneels of a
fern. fie eS
- Whether the fronds of Thamnocladus were ae on stipes
is indeterminable from the material in hand, as is also the
nature of the reproductive organs.
: The distinction of Thamnocladus clarke i from other
Paleozoic algoid forms from this country would seem a matter of
4 ~ little difficulty, as there are but few species which the plant in
; hand at all closely resembles. Buthotrephis gracilis
Hall: from the Trenton, is slender, flexuous, and slightly sug-
gests the Meshoppen specimens, but the ramules are irregularly
fasciculate, sometimes dilated upward, and generally as narrow
near the base as at the top. B. subnodosa Hall? is also
fasciculate. The aspect of fasciculationin Thamnocladus
clarkei shown on pl. 3 and 4, is due to superposition, and is
not a feature of the ramification. Even in these portions the
central strand is generally visible in Thamnocladus. The
fragment figured by Salter? as a “ dichotomous rootlet ” is some-
what suggestive of the American plant, though it is more rigid,
narrow and distantly branching like some of the more slender
examples referred to Psilophyton in America.
Thamnocladus is distinguished from Psilophyton by its lax,
flexuous, dichotomous, bushy habit, the rounded or flattened

©
<— a

ee

+
ae
——

oeal. N.Y. 1847. 1:62, pl. 21, fig: 1.

7. 1: 262, pl. 68, fig. 3. This species is generally indistinguishable by
any described characters from the group known in Hurope as Palaeochon-
drites.

* Quar. jour. geol. soc, 1858, v. 14, pl. 5, fig. 3.

_

fined, are concerned the ent ars
the Fucaceae, though = ie nee
taceae, specially Haliseris delicatula. It mé y
pared also wit the red alga Stenogramma inte |
Mont. =p
The material in hand appears to contain but ile
cate a probable relationship of the supposed seaw
orders of living algae. With respect to its habit and t
of its more or less macerated lamina the closest Fe:
would seem to be in the fucaceous Phaeophyceae, owe tl
possibility of a relationship with the higher types of Ch
phyceae should be kept in mind. Both of these great 0
together with the red algae (Rhodophyceae) appear with | Bi
doubt to have been represented by early types in the Devonie or
still older formations. 3 er
The fossils of the species here dcachiben as Thamagelaee £ ey
dus clarkei have generally been recorded in “American |
literature under the name Haliserites dechenianus
Gépp., to which the Meshoppen specimens shown in pl. D and
their associates were referred by Lesquereux. The identifica-
tion with the latter species is based on the original figures
and description given by Géppert® in his great work on the
Flora of the Transition series. The specific identity of the plant
described above with a portion of the Old World material
identified by various authors as H. dechenianus is pos-
: Fossile Flora des Uebergangsgebirges. Nova Acta Acad. C. L.-C. Nat.

Cur. Sup. vy. 22, Breslau and Bonn 1852. p. 88, pl. 2, fig. 1-6. First
named in N. Jahrb, f. Min. 1847. p. 686. :

; badly confused and questionable genus Haliserites. ©
genus Haliserites was established in 1833 by Stern
for algae with flat, membranaceous, costate fronds, with
sular sporangia grouped beside the costae in the lamina
er °¢ f the frond. The original (solitary) species proposed is
2s BH aliserites reichii? from the Cenomanian greensand
at Niederschéna in Saxony. This, the type of the genus, was
| OP ieicea by Bronn,? in 1838, to the ferns and accordingly de-
scribed as Chiropteris reichii (Stb.) on account of its
superficial characters, in agreement with that genus of ferns,
and its association with a dicotyledonous land flora. Schimper
assigned the species to the recent genus Delesseria, and Fuchs
E regarded it as a true alga, comparable to Fucus vesi-.
A -eulari s; but Rothpletz*, after examining the original speci-
: men concludes that its association with a land flora is against
its algoid nature, and that, though no lateral nerves are dis-
F cernible, it would perhaps be better to inscribe the plant as
: Phyllites reichii. Still later, Newberry in his work on .
the plants from the Amboy clays of New Jersey® describes a
3 type which he regarded as no doubt generically identical with
Sternberg’s Haliserites reichii, but for which, since
it can hardly have been an alga, he proposes the genus Fon-
tainea. It was considered by Newberry as closely related

* Versuch einer geognostisch-botanischen Darstellung der Flora der Vor-
welt. v.2, fase. 5 and 6, p. 34.

Op. cit. p. 34, pl. 24, fig. 7. “Frons stipitata, dichotime bipinnatim
ramosa, fere pedata, ramis ramulisque costatis, fere dimidiatis, latere
nhempe exteriore deficiente, ramulis oblongis, obtusis, subfalcatis, costis
eeveaue teretibus.”

*Lethaea Geognostica, 2:576, pl. 28, fig. 1.

*Traité Paléont. Vég. 1:178,

° Zeitschr. d, deutsch. geol. Gesell. 1896. 48: 904.

®°U. 8S. geol. sur. Monogr. 1895. 26:95.

- Goppert’s species, Haliserites dec an
presents a far closer resemblance yi iy ;
(Dictyopteris) has generally been made to serve as t
the genus not only among Paleozoic pei: bist ea
Mesozoic species.
The name Haliserites dechenianus was

plied? to a plant from the Spirifer sandstone, lower De 0
of Nassau. With his final description of the species G6
quotes Sternberg’s generic diagnosis verbatim. The Nz
species he describes as having flat fronds, alternate |
tomously ramose, the branches and branchlets linear, ae ee ~
width, and sometimes circinnate, the costae being n ed dian
The form and proportions of Géppert’s plant, specially in
fragments shown in pl. 2, figs. 3 and 4 of his Flora are so ainsi
to the corresponding features of Thamnocladus clarkei
_ as at first to make it seem that the plants are specifically iden-
tical. Against this, however, stand the apparently membrana- — a
ceous texture, and the generally sharply prominent costa, which |
even appears to be partially torn free in one‘ of the Nassau
types. With these differences in mind it becomes apparent
that, as artificial genera are commonly understood, Goppert’s
plant can hardly be considered as congeneric with that from
Meshoppen except we conclude it was wrongly described, and
that it is not membranaceous, not circinnate, and probably not
flat.

<<

*U. S. geol. sur. Monogr. 1895. 26:96.

*N. Jahrb. f. Min. 1847. p. 686. Jahresb. d. Ver. f. Naturk. in Herzogth,
Nassau. 1851. 7th Heft, lst Abth. p.141.

* Fossile Flora des Uebergangsgebirges. 1852. p. 88, pl. 2; see also Nova
Acta Acad, C. L.-C. Nat. Cur. Sup. 1859. 27:442.

* Loc. cit. fig. 3.

=

. same name. Among the authors who more carefully examined
i material there is difference of opinion. The Sandbergers, in their

xg great work on the fossils of the Rhenish system in Nassau,’
figure the species as a flat, membranaceous, more distantly

; bifurcating type with distinct slender median costae. The spec-
imens, occurring at numerous localities supposed by the writers
_ to be of Oriskany age, are described as having the lamina cov-
ered by a thin silky talcoid mineral, while the costa is con-
verted to graphite. The form of the illustrated segments as
well as the comments on the material appear to indicate an
algoid type apparently congeneric with Géppert’s, with which
it was specifically identified. The specimen from the lower
Devonic recently portrayed under Goppert’s name by Potonié
appears to represent exactly the same form as that shown by
the Sandbergers and seemingly belongs to the true algae, with
which it is placed by the author.

In his Fossil plants of the Devonian and Upper Silurian forma-
tions of Canada Dawson? says: “ there can be little doubt that the
species Haliserites dechenianus Gdopp., so abund-
ant in the rocks of this age in Germany, is founded on badly
preserved specimens of Psilophyton.” Carruthers,® in agree-
ment with Dawson, describes a number of apparently typical
Psilophyton fragments from the Old Red sandstone of

1 Traité Paléont. Vég. 1869. 1: 185, pl. 2, fig. 1.

* Monde d. Plantes. 1879. p. 172, fig. 2.

*Verst. d. Rhein. Schichtensyst. Nassau. 1856. p. 424, pl. 38, fig. 1.

*Lehrbuch d. Pflanzenpalaeont. 1899. p. 60, fig. 26.

5Can. geol. sur. 1871. p. 75.
*Seeman’s jour. of botany. 1873. 2:326.

—_

include, among others, Pusey y ton n robust
Dawson, Lepidodendron gaspianum Dr
nella hostinensis Stur, and the “p ant” |
Vanuxem? from the Hamilton beds near North Ney Be
Proceeding a step further, Malaise in agreement with
gian paleontologists inclines to the belief that Halise
dechenianus represents the branches of Le pido
dron gaspianum Dn., a conclusion difficult to expla
even on the assumption that Goéppert’s plant is a Psi sph ial nD.
Piedboeuf,* on the other hand, as the result of his sindioniol tee’
fragments from the quarry in the Lenne shales (upper 1 s
Devonic) in the vicinity of Graifrath, on the lower Rhine, pee
cludes that Haliserites dechenianus Gépp., Fucus
nessigii, Dawson’s Psilophyton, and Sphenopteris — =
condrusorum Gilk. belong to a single fucaceous type S a
which he calls Sargassum dechenianum. A frag- —
ment showing structure from the same quarry was studied = :
by Solis-Laubach‘ who in 1894 described and illustrated it as
Nematophyton dechenianum. aa
It is a long way from a taeniate, costate, membranaceous
alga to a branch of Lepidodendron. So wide a yariance in
correlation can hardly be explained except by the supposition
that some of the material submitted to the paleobotanists for
examination had been wrongly identified or was misinterpreted
by the writers themselves. Penhallow® in connection with the
description of some Devonic plants from New York and Pennsyl-

‘Cat, Palaeozoic Pl. Brit. mus. 1886. _p, 232.

? Geol. N. Y. 3d dist. 1842. p. 161, fig. 40.

* Mitth. d. Ver. Naturw. v. Diisseldorf. 1887. Heft 1, p. 61.

‘Jahrb. d. k. Preuss. geol. Landesanst. 1894 (1895). _p. 88, 91, pl. 2,
fig. 2-5.

*U. S. nat. mus. Proc. 1898. 16:108.

ins th Ager ecto, as due to Le ES on the ay
€ éppert of Haliserites and Psilophyton at the begin-
-epresentatives of both genera being included by him
. the same species. Penhallow regards Haliserites as an

linear ramuli with simple terminations; sporangia in groups
lateral to the midrib.” As the true Haliserites dechen-
as he describes and figures! a fragment? from Factory-
fe Wille Pa.. having the fronds regularly dichotomous at an angle of
about 40°, the divisions linear, 3mm or more in width, equally
4 i and strongly costate theese with regularly wavy or ruffled
r. margins, ,
3 _ From the foregoing it appears that the lower Devonic Hali-
-_-gerites of Géppert can not be regarded as congeneric with
Sternberg’s Cenomanian monotypic genus which is perhaps a
dicotyledon; and that great uncertainty exists among paleo-
botanists as to the nature and characters of Haliserites
dechenianus, it being regarded as a Psilophyton by
some and as a taeniate, membranaceous alga by others.. It
is evident therefore that, whether G6ppert’s plant be one or
the other, the name Haliserites. can not, without violation
of the common laws of nomenclature, be retained either for
Psilophyton or for a genus of Paleozoic thallophytes.
For the flat, taeniate, costate, linear, regularly dichotomous,
membranaceous algoid plant conforming to the genus Halise-
‘rites as defined by Penhallow? I would propose the name
- Taeniocrada. The type species of the genus is Taeni-
ocrada lesquereuxi, a specimen of which (no. 25164 of
the Lacoe collection, United States national museum) was illus-
trated as Haliserites dechenianus in the 16th volume

LON OF) ee ee ee
an 4 _ he

ame. cit. pl. 10, fig. 6.

* 25164 of the Lacoe collection, United States national museum; from the
Catskill at Factoryville Pa.

poe, elf. p. 112.

*The clause relating to the fructification should be omitted from the
generic diagnosis, since the mode of reproduction of this and the allied
Species has not been observed. |

Sr tyys a

structure. In form and aspect it is iets ar con
to the living Dictyopteris delivateiae | si i
its lamina is wavy or ruffled at the borders in addition. —
To the genus Taeniocrada would appear to belong a
specimens from the Devonic illustrated by Potonié ¢
Sandbergers,? as perhaps may the Haliserites fe t 1s
of Eichwald,’ from the Carbonic of Russia, the H. lus rtic us
of Geinitz,‘ from the Permic of Saxony, and posi = ce
lineatus and H. chondriformis of Penhallow® f om
the upper Chemung beds at Lanesboro, Susquehanna co., Pa. *
Whether the specimens illustrated by Géppert as H ali- om
serites dechenianus are congeneric with Taeniocrada, '
remains for the present a matter of doubt. “ey
Of the plants from the Mesozoic described as Haliserites
the H. contortuplicatus von der Marck® and H. =
gracilis Deb. & Ett.,7 from the Senonian, are characterized —
as membranaceous and appear to owe their reference to this _
genus to their resemblance to the living Haliseris.3 It is

* Lehrbuch d. Pflanzenpaleont. 1899. p. 60, fig. 26. bs

* Verst. d. Rhein. Schichtensyst. Nassau. 1856. p. 424, pl. 38, fig. Y

* Lethaea rossica. 1860. 1:49, pl. 1, fig. 2.

*Dyas. 1862. pt 2, p. 133, 336.

*U, S. nat. mus. Proc. 1898. 16:110, pl. 11, fig. 8b and 9.

* Palaeontographica, 1863. 11:81, pl. 13, fig. 13.

"Debey & Ettingshausen. Urweltliche Thallophyten. 1859. p. 61, pl. 1,
fig. 1, 2.

* Other Mesozoic species described as Haliserites are: H. schlotheimi
Debey (Entwurtf. e. geogn. geogen. Darstell. d. Gegend vy. Aachen. 1849.
p. $1) and H. trifidus Debey (Verh. Naturh. Ver. pr. Rheinl. u. West-
phil. Jahrg. 5. 1848. p. 114) from the Senonian; H. tunguscanus
Schmalhausen (Mém. Acad. imp. Sci. St Petersb. Ser. 7. 27:59) from the
Oolite; and H.? elongatus Fr. Braun (Miinster’s Belitriige. 1848. v. 6,
no. 26, p. 26) from the older Mesozoic.

op rat 6 or to the algae with Se Rae ee daaninae seems

‘await thorough examination of the original specimens

gether with other material from the type locality or local-—

P ities. It appears not improbable that Psilophyton will be.

z found at the same stage and perhaps at the same localities.

_ On the other hand it would not be strange if in the Psilophyton

group, the doubts as to whose supposed structure were pointed

out by Solms-Laubach?, we should find transitional types be-
tween the algae and ferns and even other classes. And it |

- should be borne in mind that such forms as Thamnocladus

4 clarkei, while presenting the general aspect of many ordi-

-.: nary seaweeds, particularly among the fucaceous Phaeophyceae,

and containing structural traces strongly suggestive of a some-

: _ what highly organized axis, may eventually prove to be allied
to Nematophycus (Prototaxites) or to some higher type.

. The Devonic period offers a most fascinating as well as diffi-
cult field for paleobotanical investigations; and it has great
need of ability and experience of the highest order to conscien-
tiously and patiently work out the elements of its plant life,
making the most of its generally scanty and obscure plant re-
mains which must sooner or later throw the greatest light on
the paleontologic origin of the ferns, equiseta, lycopods and
gymnosperms.

*It would seem that in such instances the ancient types should receive
. Some distinctive name, such perhaps as was given to the Paleozoic forms of
Chondrites which Schimper designated (Zittel. Handb. Palaecont. 2:61)
Palaeochondrites.
* Jahrb. d. k. Pr. geol. Landesanst. 1894 (1895). p. 74, 77.

the whens of Melrose, Benagelnck: co. N. ee vin the e
1901, Dr. R. Ruedemann uncovered a remarkable s
graptolite faunas representing the associations eS thos orgi
isms found and heretofore described by Hall and others )
the shales of the Quebec formation at Point Levis
Anne in Canada. Of this interesting occurrence -
very important measure to our knowledge of the
of New York, Dr Ruedemann has already given a ] a ?
account in this report, with a summary of the a iat
and vertical distribution of the graptolites. These gra
lite-bearing horizons, three in number in the section exposed, ¢
black shales interbedded with green grits and gray sands, a and, —
while they have produced graptolites in ~ profusion a vi:
variety, other organisms prove to be very quent; so me
small oboloids like Paterula, two specimens of a great Lingola,
the largest known from the Paleozoic, which approaches. ins
general features L. quebecensis Billings from the Point —
Levis section, and several examples of a very large shell in FY
which we recognize an interesting new type of brachiopod struc- — a
ture and purpose to describe under the generic name ae

EUNOA ae
Inarticulate, subcircular, disk-shaped shells of discinoid ex- _
pression. Brachial valve slightly convex with apex situated
between the center and posterior margin of the valve; pedicle
valve flat with wide open triangular foramen having its apex at
the center of the disk and with margins rapidly diverging to
the periphery. Shell thin, chitinous, phosphatic; surface with
raised concentric filiform lines and finer radial intralaminar
striae.

“outline ‘normally subeireular or trang. si

ae

lines ons Por wad eo the apex and seen best

: ES. st fates of muscular scars similar to such as are _
frequently displayed eases of the genus Orbiculoidea. The

specimens indicate an ebieur and short peripheral notch or
_ineurvature on the posterior edge.
In the pedicle valve the cleft is wide, and its apex nearly
central. The edges of this cleft show convergent, thickened
: == shell ridges, which lie just within the margins and unite at some
- distance in front of the apex, becoming thicker and more highly
FE raised, thence continuing forward for a short distance as a
~ single ridge, which soon fades out on the pallial surface. In
_ the existence of these muscular fulcra we find again a parallel
pestuon to that seen in many orbiculoids.
_ The shell substance is highly tenuous but seems to show a
. eubdivision into two layers. Doubtless here, as in the cases of
such brachiopods elsewhere observed in bituminous shales, the
original lime content of the shell has been lost in fossiliza-
tion; however, this lime content must have been slight and
greatly subordinate to the phosphatic element.
These shells are all large, indeed the species is one of the
largest of the inarticulate brachiopods. On bringing this genus
into comparison with known allied genera, we observe that its
differentials from those are as follows.

In Orbiculoidea, the wide open pedicle cleft is an embry-
onal and nepionic condition in all species where the ontogenic
development has progressed normally. In Schizocrania it
is a normal adult phase, but Trematis is a heavier lime-shelled
genus” with other differentials expressed in the submar-
ginal apex of the brachial valve and in the ornament of the sur-
face. Trematis likewise maintains the open foraminal fissure

Neaienang, “under compression appearing somewhat
by abe curves at the side. Brachial valve with low

i ; perigee each h ot ark eee
it PAC Shaal Sa oe oh Fn set Tee
ep" ese two g : bao
pressions of Orbiculoidea. m8d schizobolus
pedicle‘passage is a very short tri riangular
a late survival of the primitive stage re '
Trematobolus, Schizambon mc 0 -
which the pedicle has not only become poms
sheathed by a short tube. gn ee
The generic characters of the genus Fuitos * are th us 5 W
defined, and no other shell carries so primitive an exy . oss ion
of the orbiculoid type, a highly phosphatic shell, a ia
triangular pedicle cleft and unmodified concentric surfs ise _
ornament. Pi.
Horizon and locality. In graptolite shales of the age ¢ of
the Beekmantown limestone, on Deep kill near Melrose N. ° i
Observations. The striking similarity of this organism se 2
that described by Jones and Woodward from the Moffat shales
of Dumfriesshire as Discinocaris gigantea leadstoa — ~
few remarks which are naturally suggested by this resemblance. rt
Moffat series. The Moffat series of Dumfriesshire which has _
been described in great detail by Lapworth!, is constituted of
black bituminous shale bands with interbedded grits, the former
carrying extensive graptolite faunules with such forms as a
Monograptus, Dicranograptus, Climacograptus, Dicellograptus,
Pleurograptus, Leptograptus, Thamnograptus and many other
genera which are present in the Deep kill section. Lapworth
has found evidence for regarding the comparatively slight thick-
ness of these beds as a sedimentary equivalent in the section
where they occur, of the Siluric series from the middle of the
Llandeilo up to the Wenlock, basing this deduction chiefly on the
range and limitations of the graptolite faunas. There is herein
# condition clearly parallel to that now determined for the
Hudson river beds of eastern New York, whose graptolites have

‘See specially Lapworth. The Moffat series. Quar. jour. geol. soc.
1878. 34:240-346,

Se iralod their equivalence to sediments elsewhere
ing from the middle Trenton upward to the top of the
ine shales. From these Moffat beds and in association
| some of the graptolites, Prof. T. R. Jones and Dr H. Wood-
d have described a number of circular shields of chitinous
tance, concentric markings and triangular cleft, as crusta-

: -ceans under the name of Discinocaris. ‘The type species of this

A

A group of putative phyllopods is D. browniana; and among
them is the large shield to which we have referred, Discino-
‘ earis gigantea. Examination of the figure with restored
E outline given by these authors, which we reproduce here, shows

|. wf eed. eee

Discinocaris gigantea after Jones and Woodward

evidence of the convergent internal ridges showing through or
impressed on the surface ornament and corresponding to these
well marked muscular characters in Eunoa. This specimen
is apparently the most nearly entire of any recorded; but the
authors note that fragments of these bodies indicate a diam-
eter of- fully 7 inches. That Eunoa is a brachiopod of which
we have both valves is beyond contest; and that Discino-
caris gigantea, occurring in homotaxial rocks of similar
character formed under like bathymetric conditions and with

_

These organisms are all aa
cordate shields, bearing a deep silanigitie elite
ing back to the apex of the shell, about over
lines are concentric. These bodies abound at certé in Deve
horizons, and some of allied form were early observed y
Roemer and de Verneuil, who, familiar with the apty
Ammonites in the mesozoic, designated them without.
closer investigation, as aptychi of the Goniatites. — CMe
Discinocaris was described by Woodward; and, th a
its forms, of which a number have been named, are in t :
tures mentioned above not materially unlike the cna i
jects Spathiocaris and Cardiocaris, they are for the most p
from horizons which long antedate the appearance of the ¢
tites. We have shown that one is evidently a brachiopod 3
large size, but this is one of the most recently described
referred to the genus. a
The genus Spathiocaris was described by the writer. Follow-
ing H. Woodward’s determination of D. brownianaete.as
crustaceans, Spathiocaris (Naples fauna) was also referred to |
this group of organisms. | wee a
Soon after describing the genus (S.emerso ni), the writer
referred similar bodies from the Devonic at Bicken, West-
phalia, to Spathiocaris and Cardiocaris, regarding them as crus-
tacea. Kayser at about the time of this publication, had
discovered and described some of these bodies from Bicken
as occurring in, though not well fitting, the body chamber
of the goniatite, Manticoceras intumescens. Simi-
lar occurrence was noted by Woodward in a goniatite from

a Eeatial plate, that the others were rationally saaaeanke
e crustacea. — . a

Bee cicmentary to hie deubsiohion of the Ganialiles
‘the Domanik schiefer. It was from these shales that de
‘erneuil described the first known of these bodies as aptychus
f a goniatite. Holzapfel, in rehearsing all the evidence in
: more detail than is given in the foregoing and without attempt-
ing to enter upon an analysis of possible crustacean structure,
concludes that at any rate Spathiocaris and Cardiocaris
were not aptychi or ammonoid operculums. That they may
not have had some other function in the ammonoid body.
he is not disposed to deny. From so high an authority on the
SS ¥ structure of the goniatites this opinion carries much weight;
and Holzapfel reiterates the statement by de Verneuil that
these bodies occurring in the black layers of the Domanik
schiefer are not immediately associated with goniatite shells.

feature of the occurrence of these bodies in the Naples and
Genesee beds of New York, where, after 25 years of search and
the acquisition of hundreds of spathiocarids, in no instance
has any specimen been observed in association close enough
to suggest, of itself, any relation to the ammonoids. We are
now speaking of the singly cleft shields, such as have been in
two recorded instances found within the goniatite chambers in
the limestones of Germany, as above referred to.

id
| The writer has repeatedly drawn attention to the same
;
‘
~
j
;

Here is evidence of affinity which points both ways. To prove
these bodies opercular shie’ds or covers for any other parts of

_

"

By
on.

In meeting these obstacles it is to be borne in mind the
gle specimen of any of the genera Discinocaris, Pho
Spathiocaris, Cardiocaris has been proved oe a: e ‘he s
ments and spines referred to these may or may not h
relation to the shields themselves. ne
There is a series of these shields which is uli
specially mentioned above, in having a triangular cleft i
extremities, that behind not reaching to the apex or gr

These are wholly inten objects and have heen ter Bes
by the writer Dipterocaris. American specimens have —
found not so much in the bituminous layers of the upper
Devonie as in the flags and sands, and certain specimens eG if
clearly indicated that in uncompressed condition the contour —
was distinctly sloping from the bridge between the two latera’
wings of the shield. Among these specimens there is no aaa «
for any suspicion that they have brachiopodous affinities.
Regarded as crustacea, that is Phyllocarida, at the time of the
description of the genus, the crustacean similarities are indeed
more strongly marked than in the Spathiocaris class of
shields, a feature specially brought out on comparison between
such a Dipterocaris and the carapace of a phyllocarid like’
Rhinocaris or Mesothyra; but on the other hand the gen-
eral form, structure and surface characters of all these

RZ ’

‘ae

x

F _ the waves unable to transport the heavy shells, and have hence
a been accumulated by themselves in other sediments than the
latter; a plausible contention could we but find some more
satisfactory ground in the structure of the “aptychi” for
ascribing this cephalopod function to them. :

In the Paleontology of New -York, v.7, we figured the sole

Ee
>

{ rest, the 1 more as they are eee in : the rock |
i: ‘Yet in these bipartite shields we find a closer analogy, —
to the ammonoid aptychi of the Mesozoic, so far as the
n of the shield is concerned. It has been argued by
us writers that the tenuous chitinous substance of these
dies is purely a result of preservation. Calcareous substance
; frequently destroyed in bituminous shales; hence the ecal-
areous layers of these bodies may have been thus removed,

sate only the organic film. Specimens from the sandstones
are however equally devoid of trace of calcareous layer. It has

_ furthermore been contended that these presumable aptychi, on
the decomposition of the animal’s body, have been floated by

instance known from the rocks of this state of the concurrence
of any of these bipartite bodies with a goniatite. Here is a
specimen from the soft Naples shales, presenting a body
whorl of Manticoceras pattersoni, the diameter of
whose shell originally was not less than 3 inches. On and with-
in its body chamber lies a Dipterocaris or at least an object
having the doubly cleft outline of the species so denominated.
This little body has a length of about 5mm. This concurrence
may, of course, be quite as casual as the usual dissociation of
these bodies. If, however, this be taken as an indication of
relationship between the ammonoid and the Dipterocaris,
it is not the relation of aptychus or operculum. However, in
view of all the present evidence, we can not divest ourselves
of the belief that there is nevertheless some organic connection
between these Devonic bodies and the cephalopods; for, while
we lack any further confirmation of the latter than that above

—

pe Portage group in the Tannery gt ally ¢ é

has produced a number of sing) la obje pjects, Pa ro]
eryptophya, some undescribed rephyre ee
unrecorded occurrences. This object is one half. ;
shield resembling a circular Spathiocaris or Care lic Paris.

In the collections of the state museum there “has Re

sketch, of a large discinoid body taken from the
of the upper Devonic (Portage stage) at Truxton, €
both cast and drawing sent to the late Prof. Hall es
Rey. H. A. Riley of Montrose Pa., a well known colle “4
student of fossil organisms. It will be observed — from t t
accompanying figure of this body that the furrow which ¢ om ses
the surface of the body is accidental, not natural, as it eae Or H) %
divides the body into unequal parts but is crossed by the concen- ve:
tric rings of growth. The body was originally depressed conica il,
as shown by the irregular wrinkling of the surface under com:
pression, the beak being well forward of the center and the con- 2 .
centric lines conspicuous but not relatively so to the size. The
dimensions of this object are specially noteworthy; fore and aft }
it was not less than 5 inches long and transversely through the is
center nearly 6 inches. The Naples shield has just about the .
same dimensions. Either of these bodies by itself fails to
explain its true nature; taken together, I am disposed to believe
that all the evidence indicates that the one is probably the cor-
relate of the other, one a pedicle valve, the other a brachial — “4
valve of a great inarticulate brachiopod like Eunoa. We should —
probably go astray in identifying this great shield generically
with Eunoa from the Melrose graptolite beds; and in view of

eo.

aes ee a

~~ ay

a

Orbiculoidea magnifica

Upper or brachial valve

Since this article was put in pages the specimen here figured has been
obtained from the Tannery gully at Naples, the same locality and horizon
which furnished the folded pedicle valve shown on plate 7. The presump-
tion made in the paper that that body appertained to a discinoid brachio-
pod is thus fully justified by this recent acquisition.

~— esee shales in the valley of the

This group presents an extensive Pacusiph pm
and flagstones, and finally, some thick 1
toward the upper part. Like all the other mecha
of the system, as they appear in New York,
__-variable in character at different and distant
- From its superior development along the ba
river in the district formerly included in the to ci
now Portage, it has received that name to ating
the higher rocks, which possess some differences i 7” ]
characters, but a more striking wie eee in orga uni

upward order 1) Cashaqua shale, 2) Gardeau a
stones, 3) Portage sandstones.”

The footnote accompanying the woodcut says: “As wi :
from this point, however, there is a constant increase pe
naceous matter, and in a westerly direction an increase of n
or shale.” ir a ‘a

The strata that compose the Portage group as thus defined —
are exposed almost continuously in the sides of the deep canyon |
of the Genesee river from near its opening into the wide a .
near Mt Morris, to the top of the cliffs on the south side of the EL
high railroad bridge at Portageville, a distance of 15 miles in
a direct line, and about 20 along the tortuous river channel. e
The difference in elevation between these points is 680 feet, and ,
the dip adds 381 feet to the rock section; total thickness 1061

feet. . ,

in $10 continuous Hes It is eee seat int 6
ust of the Genesee gorge on Cashaqua creek and can be
traced westward to Lake Erie and eastward to Seneca
throughout the entire distance it is found to overlie a
of black shale in which fossils are exceedingly rare. In the
_yiver section this bed is about 35 feet thick. This has been
reed the lower black band and is continuous and well de-
‘fined from the Naples valley on the west to Lake Erie, increas-
& slowly in thickness.

a Next below, and overlying typical upper Genesee shale, are
an to 6 feet of lighter colored shales and a few thin flags, the
a whole bearing a much closer clastic and paleontologic resem-
blance to the Cashaqua shales than to the dark gray shales
bearing Lunulicardium fragile abundantly, on which
= they rest.

Overlying the Cashaqua beds occurs another thick mass of
densely black slaty shale, known as the second black band. It
is of the same character as, and coextensive with the lower
mass and like it increases in thickness toward the west, while

* the Cashaqua shales decrease in that direction. These two
| black bands are bench marks in the stratigraphy of the Portage
. Sections as their character is maintained and they are easily
recognized for more than one hundred miles east and west of

the typical section, while the other beds are variable in char-
acter and not to be distinguished without much care and study.

The second of Hall’s divisions, the “ Gardeau shale and flag-

stones ” was described (p. 227) as “a great development of green

and black shales with thin layers of sandstone.” It includes

the second black band which is its basal stratum. The upper
limit was not definitely given, as the only change noted in the
character of the sedimentation is the increase of arenaceous
matter toward the top. ‘ Towards the upper part the courses

- fall at “igen: (10s A. ™) is = oe

and the southward dip adds 208° (eet, es
feet for the thickness of the Gardeau divi

With regard to the Portage sandstones; Dr Risin
“The thick bedded sandstones at Portage form thel !
rocks of the group. . . The upper part counts of
bedded sandstones with little shale, while below
ers become thinner, with more frequent siternatiegeal of sl

There are 182 feet of strata embraced in the section pet
the assumed base 27 feet above the upper fall and the t¢ op of |
the cliff south of the bridge and on the east side of the 1 bens .
A layer of hard blue shale, 2 feet thick, occurs 12 feet =
this assumed base, and another of similar character is— fo
52 feet higher; very thin shaly partings also separate some of
the harder layers, but with these slight exceptions the forma-— me
tion consists of layers of light bluish gray, medium fine elned NG
sandstone from 2 to 10 feet thick. The character of the rock —
is remarkably uniform, varying but slightly in the degree bee)
hardness, some layers showing a tendency to be schistose or
flaggy; occasional concretions occur. G5 4

“The Portage sandstone is succeeded by olive shaly sandstone - a
and shale and this by black micaceous slaty shale with septaria;
to this follow shales and coarse sandstones with fossils of the
Chemung group” (Hall, p. 248). These beds are not exposed
along the river but the lower portion may be seen in the
ravine of Wolf creek below Hopkins’s mill at Castile, and the
upper part in the ravine of West Coy creek at Wiscoy, and in

ore cap ‘the ues auatanck ana still retain
eristic species of the rocks below have been termed

arke ‘the aati, beds. They are composed mainly of soft

bluish and argillaceous, or olive and sandy, with ocea-

thin black layers, a few flags or thin sandstones and

reous concretions. :

ty ‘They are terminated by a band of flags and thin sandstones

ze the at appear in the north wall of the ravine above the falls at

_ Wiscoy, and in the sides and bottom of the river channel a mile
- south of Fillmore where they form “ Long Beards riffs.”

3 _ These latter sandstones are about 150 feet above the Portage

ae of the Chemung group” that have been found in the immediate
s a vicinity of the Genesee river. They are succeeded by nearly
~300 feet of shales and flags and these are overlain by the heavy
Rushford sandstones, exposed in the hills west of Caneadea.
a: Chemung fossils are common through this mass of shales and
sandstones. :

The Portage sandstones in the Genesee river are therefore
separated from any lithologically similar formation for 450 feet
above and none of like character of sufficient thickness to cause
confusion in correlation, occurs below.

Recapitulating, the subdivisions of the rocks of the Portage
group in this section, that by their individual characteristics,
their homogeneity and their thickness are so well defined that
they may with safety be used in correlation with other local
sections, are: the lower black band, 35 feet, the Cashaqua shale,
130 feet, the second black band, 52 feet, the Portage sandstones,
182 feet.

Besides these, there occurs in the lower part of the Gardeau
beds, interstratified between beds of shale, a band of flags and
thin sandstones aggregating about 25 feet in thickness, that
becomes a more distinct feature in the stratigraphy toward the
east, and will be referred to again in this paper.

_—

sandstones and are the lowest “coarse sandstones with fossils ae

ti carried over ‘inte tha h
me ~ another may have survived the gener
fauna from the east.
In the town of Naples, about 30, valle uae ft
river the upper beds of the Genesee shale, all of #
divisions and several hundred feet of lower, Chemuzig D
the aggregate not less than 1500 feet, are abundée ntly.
in the numerous ravines and rock escarpments about th
end of the Naples valley. . ‘ é |
In the strata above the Genesee shale the proportio y n of
sediment, in the shape of flags and thin sandstones is n roti
greater than in the Genesee river section, and the aaa ke >
the subdivisions is not the same, still the differences in Ii i

logie character are so small, that no diffi ulty is Nees ed in|
distinguishing the several subdivisions as previously descr qd.
The upper beds of the Genesee, succeeded by the nace af
lighter colored shales and flags, and next above, the lower black —
band are exposed along the road leading westward on the —
Naples-Bristol town line near Woodville and near the mouth of —
the Snyder gully, { mile south. | re
The top of the Genesee shale in the road west of Woodville is 7
A.T. This point as indicated on the Naples sheet of the 4
topographic map is on the line of 42° 40’ which crosses the —
Genesee river 5 miles south of the mouth of the gorge at Mt
Morris and almost exactly at the place where the top of the
Oashaqua shale dips below the river level, which is here 6027
A.T. The top of the Genesee shale at Woodville is therefore
the difference in levels, 149 feet, plus the thickness of the-

te score ‘the hillsides ‘between ee ie ea ieee
ge of. Naples. The beds are quite sandy, flags being

wer, and it is also more fossiliferous, the characteristic
fossils of the group being quite common in the softer shales.

_ The second black band, less than half as thick as in the Gen-
» river section, but well defined and easily distinguished is
ex ed in the same ravines, and also in the rock cut on Rhine
_ et, and at the foot of Hatch hill, opposite the village of
Naples, where it dips under the water of Naples creek at about
& ig A.T.

peebandantly exposed at the tout of Hatch hill, and in the
Rainer parts of the ravines at the north, but much better in the
x as Diecinery gully, 1 mile south, and the Grimes gully $ mile west of
the village, there are about 300 feet of shale and flags that cor-
2 _ respond very closely, both in structure and fossils, to the Lower
_ Gardeau beds as they appear in the escarpments between Smoky
hollow and the top of the upper Portage fall. The shales are

‘
a
Pt

bluish gray with different degrees of hardness. At some hori-

eee |

zons the proportion of arenaceous matter is very small, while
P at others it is equal to the argillaceous.

At the top of these beds, and about 600 feet above the Gen-
esee shale a series of sandstones, varying in thickness from an
inch to 8 feet, and separated from each other by thin shaly
partings, and aggregating about 50 feet thick, produce the third
falls in the Grimes gully, the High falls in the Tannery gully,

and prominent escarpments on the sides of Hatch hill and West

hill. They are known as the Grimes sandstones. Their most
southern exposure is on Olney brook at the waterworks reser-
yoir 14 miles south of Naples, at the elevation of 975’ to 1025’

n and a few layers of sandstone reach a foot in thick- |
The upper part is more argillaceous and calcareous than

black, bluish or olive, in all varieties, and the sandstones light

Ee z “the sides of the. vie ae es Ph. FS eeaee
The proportion of. aie ‘setinent i “the Grin les
as in the flag and shale beds below, is much Ie sin th ch
tion, but the formation maintains its character ¢ suffi
noticeable as a distinct band of flags and thin sandston
cliffs on the east side of the river at St Helena, and a Us
southwest, where it comes down to the river level nett
of Wolf creek, almost exactly west of the exposure at:
voir in Naples, at the elevation of 675’ to 700’ A. T. _ 95:
Up to the base of the Grimes sandstones the sanity i in oth
lithologic and paleontologic aspects of the two section as makes
correlation simple but at this horizon, in the Naples sectior n, th ar’
Portage fauna suddenly and finally disappears, while i ins n th e
Genesee section it holds its place to the exclusion of all I rach hio- —
pods to a horizon that, stratigraphically, is 700’ to 800’ Mowe i 4
The last appearance of the normal] Portage fauna in the Na =|
section is in some thin layers of soft shale between flags, in oy
face of the precipice at the third falls in Grimes gully, and this
fauna is found also in similar shales at the same horizon in Tan- © a
nery gully at the High falls. aes
~4 feet higher and 9 feet below the crest of the falls a 4 inch ra ;
layer of soft sandstone contains Liorhynchus quadri- er
costatus, Atrypa reticularis, Productella
speciosa, Ambocoelia umbonata var. gre-
garia, Leptostrophia mucronata and Orbicu-
loidea sp., an assemblage regarded by Clarke as altogether
foreign to the Portage or Naples fauna. These fossils are found
along the line of outcrop of this layer for four or five rods on both

id -
Mey: ¥

ne . but Sapeat to be barren of fossils. ‘They are ex-
na similar manner at the as of the High falls in the ©

ra foot thick is composed principally of crinoidal segments
‘comminuted brachiopods and shows a few specimens of
orhynchus, Atrypa, Productella, Ambocoelia umbo-
: rata a and a small Chonetes in a recognizable condition.

e gts pe orrens fenra extends 60 to 80 rods aes the north

Ee Ei up Hatch hill. A few feet ioe occur species of the
dictyosponge 7 Hydnoceras with Paropsonem a er ypto-
f -phya, a large Orbiculoidea and other problematic organisms
_ notelsewhere seen. A Leptodesma of notable size and not seen
f= in the beds below occurs in the lower part of the Grimes sand-
_ stones in the small Smith ravine south of the Tannery gully and
also in a field outcrop in Nellis’s pasture 14 miles northeast of
the village. The same fossil appears on the surface of a thin
sandstone about 50 feet above the Grimes sandstones in the
Lincoln gully on the opposite side of the valley. Sponges,
crinoids and a few brachiopods have been found in these sand-
stones at several other outcrops in the valley.

The Grimes sandstones are succeeded by shale, flags and thin
sandstones in varying proportions for about 600 feet to the base
of the High Point sandstones. Very few of the harder layers
reach a foot in thickness and no distinctly sandy band is of suf-
ficient magnitude to assist or confuse in the determination of
horizons. No layers have been found to be continuously fossilif-
erous, but many of the sandstones and a few of the shaly beds
contain fossils quite abundantly for a short distanee,

Of the fossils observed in the strata between the Grimes ‘gana.
stone and the High Point sandstone the following are note-
worthy.

-

So a eee da

—

2M Wee iis Yates rarer a
2435 Powell hill, 25 miles north 0
Siivinies sandstone |
Ambocoelia umbonata, 2450, 2431, 2482 2433, Deyo ba basi
feet above Grimes sandstone 7 a ime
Spirifer mucronatus var. posterus, — 2431, 2433, Di yo

S. mesastrialis, 2432, Vs Sp aie oe ae ae
S. disjunctus, Deyo basin A ee a
Stropheodonta cayuta, 2431, 2432 | a

Schizophoria impressa, 2451

Atrypa hystrix, 2431, 2432, Deyo basin

Productella lachrymosa, 2432, Deyo basin

Liorhynchus mesacostalis, 2433

Grammysia elliptica, 2430, 2433

Cimitaria corrugata, 2430

Leptodesma robustum, 2431

Palaeotrochus praecursor, 2432 -

Hydriodictya cylix, Deyo basin :

Ceratodicetya annulata, Deyo basin

Hydnoceras tuberosum, 2434

H. variabile, Deyo basin 0. a ae
Arthracantha depressa, 2429, Deyo basin Rotate 6,
The flags and shales in which these brachiopodous faunules— Zs

are found are stratigraphically equivalent to that part of the — fi

Gardeau flags and shales exposed on the Genesee river between —

Wolf creek and the top of the upper Portage falls. Structurally

they differ very little from the undoubted Portage beds below, |

or the equally unquestioned Chemung strata above them.

tigraphic position corresponding to that of the Portage sand-
aes ‘at ahs The outcroppings of these pana ness

Ps. ee en accurate measurement of the: strata composing
it is not practicable, but the heavy layers of sandstone are promi-
nent in the bedding for 150 to 200 feet, closely resembling the
-Portageville rocks, but more frequent!y separated by beds of
shale. The largest and most favorable exposure is in the cliff
at High Point 2 miles west of Naples, at the elevation of 1700’ to
1800’ A. T., where about 75 feet of the sandstones and shaly part-
ings appear in place in the escarpment and large blocks are scat-

=

A chee y cm ss
ie

= ae

tered over the immense talus.
Situated about the middle of the section exposed is a calcareous
lens 5 feet thick at the center, and 25 rods in breadth, composed

ee ee en eae ere ee

almost entirely of fossils, of which 33 species have been identi- —
fied (United States geological survey, Bulletin 16), 24 being
brachiopods, none of which so far as known have been found in
the Portage section on the Genesee river, nor below the Grimes
sandstones in the Naples section. This constitutes tle interest-
ing High Point fauna which has been elsewhere described and
shown to carry a marked representation of species present in the
upper Devonic faunas of Iowa.

No fossils have been Apt bop eae roe
Station 3. 4 mile east of station 2, on the
hill. An escarpment in which is a thin ealea: eous la}
posed principally of crinoid stems and bryo: 202 =
many brachiopods. any
Station 4. Ledges on the west gide of Knapp hill, 4 Ah
southeast from High Point. A caleareous concretior ar, ‘y lay
crowded with D. tuberosum and Chemung br hi
Station 5. One mile east of station 4 the sandste
in several small escarpments on north slope of Pine hil, — 7
Station 6. McClarries’s quarry on the hillside east. of th ‘
lage of North Cohocton. About 30 feet of light blue g :
pact sandstones in heavy layers are exposed. A thin see n 0
shale in one of the hard layers contains a few small veo re ds |
No other fossils appear. This quarry is evidently in the Por a
sandstones but its stratigraphic position in them is not cert nly ‘
known. It is 5 miles directly south of High Point and 30 miles
east and 1 mile north of the cliff at Pertageville. The altitude a)
is 1575’ to 1600’ A. T., indicating an elevation of 300 feet to 400

feet or a westerly dip of 10 feet to 18 feet a mile, anda southward > 4

ox
ni

3

dip of 25-30 feet a mile. ;
Station 7. A small exposure near the foot of the hill on the
north side of the road leading from North Cohocton to Wayland, )
a littl east of Dotys Corners. It is about 4 miles west from
station 6 and there is not much difference of altitude. A cal ‘
careous layer, similar to the one at High Point, but thinner, is ae
composed of Chmeung brachiopods.

Station 8. Quarry 2 miles west of Wayland on the north side
of the road to Dansville. Altitude about 1400’ A.T. No fossi's
have been observed here.

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aA quarry is 18 miles due east of owt

upper | part of the f formation. . “alti

fossils observed were a small <2
stems and plates, plant remains and

Hydnoceras tuberosum and a few brs —_
in a layer of flaggy sandstone that outcrops 1 mile f fa
and 325 feet lower. aA

Station 10. Exposure along the Pittsburg, SI : ymut
Northern railroad between 3 and 4 miles south of station a
1 mile north of Rogersville station. About 50 feet of | he
sandstones outcrop in this vicinity. No fossils observed he ar€

Station 11. In Stony brook and two small lateral envtml boat at
a mile south of the high Stony Brook bridge. H ydno cera
tuberosum occurs in the lower part of the sandstones e: a
posed in the main ravine below the highway bridge. a > ;

In the Stony Brook ravine at the high bridge and below toi
mouth, about 375 feet of strata are exposed. They show no ap:
preciable difference in lithologic character nor in the contained -
fossils from the same horizon in the river sections. No brachio
pods were observed here but the normal Portage fauna is found —
in the soft layers.

Station 12. An exposure of about 50 feet of the sandstones $ ~
mile east of the village of Byersville, in which a thin layer
afforded several specimens of Atrypa aspera, a small —
Orthis, Cladochonus, ete. :

Station 13. The outcrops on Quarry hill, 1 mile south of the ‘
village of Nunda. About 35 feet of the sandstones are exposed —
and a shale bed 6 feet thick of the same character as the one ~
occurring a little below the middle of the sandstones at Port- —
ageville. A few goniatites and orthoceratites have been found ©
in this shale, and about 25 feet higher a mass of crinoid stems .
and comminuted shells, in which only a small Chonetes is entire, —

oe 52

-

ving Wiscoy shales in the Genesee river section, the normal
ge fauna continued to hold the ground while in the Naples
on at the beginning of this period the succeeding fauna had
oe from the east, Shag ais gt itself and remained, driv-

% Wi, and Saabs § peoken by periods of recession, for in all
t time it covered but 25 of the 30 miles between the two
sections. |

eo, 6 6the upper limit of range of the Portage fauna descends in
the strata, very irregularly doubtless, from the top of the Wis-
_ coy shales above Portageville to the bottom of the Grimes sand-
stones at Naples, a vertical decline in the strata of 760 feet in
a distance of 30 miles. |

i

Point sandstone, ak eat ) ee mstrued as a
fauna. The list of species cited Apr’ ciao
contains species which in a measure occur in € mu
but Spirifer disjunctus is ahead )
Point horizon and none of the molluscan species a
to the higher Ithaca fauna pertaining to the Por age 2 ™ "OV
adjacent on the east. The frequent Dictyosponges a ‘me
Chemung habit but these bodies (Hydnoceras, “tea 2 of t the
foothold in western New York directly after the disapy are a 1
of the Naples fauna, and did not become freely dissemin:
the more eastern Chemung deposits. Thus in the correl:
of the faunas of the Naples section with those of the Ge nese |
river we may say with approximate accuracy that in the latt er
the Naples or typical Portage fauna ranges through all beds”
from the top of the Genesee shales to the top of the Wiscoy
shales (Cashaqua, Gardeau, Portage, Wiscoy), a thickness of
1211 feet. In the Naples section this fauna first appears briefly —
in the Genesee shales, temporarily disappears, reappears with
the deposition of the Cashaqua shale and continues through a
thickness of 600 feet of sediment. It is then driven out by an |
invasion from the east of the Ithaca fauna which held the field
while the sediments equivalent to the middle and later parts
of the Gardeau flags were deposited, and this congeries pene-—
trated part way across the interval but did not reach the Gen- |
esee valley. Compared with the eastern development of the —
fauna in its proper province, it was comparatively few both in ;
species and individuals. After holding the field during the most —
of the stage of Gardeau deposition it was displaced by the
incursion of the Chemung fauna with Spirifer dis- q

junctus, whose earliest presence was contemporaneous with —
the desposition of the Portage sandstones. This fauna did not
reach the Genesee river till, as stated by Mr Luther, the horizon ~

a S ae = aia

os Pee see | é
ag -Long Beards riffs - “ poe
ral) ae be died ; “shiv
Wiscoy

Pic a 5 .

ee Grimes
Gardeau . sandstone

- Naples
shales
(Cashaquaé

Sipe)

NAPLES
NAPLES FAUNA

rnd |
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Eawhich we hope to publish before the dice of another year.
For more than half a century the problems for which it is be-

¥ - Tieved a rational solution is herewith tendered, have engaged the

_ attention of North American geologists. All who have worked

. 7 on any part of the Appalachian region have observed a great

difference in the stratigraphic succession as soon as they

-- entered the area lying just west of the Appalachian protaxis.

4 ea However careful their investigations, something has remained to
an:

be explained, and many ingenious suggestions were offered, with-

_ out, save obscurely in one instance, attaining the true solution.

Ss Stratigraphic continuity was assumed, and the more fragmental
character of the sediments along the western flank of the pro-
taxis was believed to indicate little more than proximity to the |
- eastern shore line of the interior sea, while the interruption in
the gradual change eastward in the character of the deposits
_ was generally ascribed to overthrust faulting.

But these explanations satisfied neither the stratigrapher nor
the paleontologist, and they were accepted only because no bet-
ter solution of the difficulties was at hand. The fact is, they
did not explain and were mere makeshifts, necessitating one
assumption after another as detailed mapping progressed.

Apparently the accepted solution did not satisfy that excellent

stratigrapher, Sir William Logan, who, in checking the results of.

his investigations, enjoyed the advantage of close association
with so careful and able a paleontologist as E. Billings. With
a little more light Logan might have grasped the full signifi-

cance of the stratigraphic discordance prevailing so constantly

*Published by permission of the director of the U. S. geological survey

and of the secretary of the Smithsonian institution.

—

oll lowing brie ae - spe results of a series sof ee

Rare

Plate 9

AN

yy
Mi

Map showing Paleozoic barriers in eastern North America.

a 8 866, that this oy D) th Pe a ciceee et
a we regard the correlations based on this view by y Log
as the data from which the idea itself grew, an 8 Dein
ance with the facts, his suggestion of distinct basins sit s 3
us, was far too important to deserve the oblivion t
has been assigned for all these years.’ : | “a

Though abundant corroborative evidence of the € ae 0:
narrow barrier between the stratigraphically inh arn onio
areas is afforded by the structural geology of the region i
question, it was perhaps scarcely to be expected that the ge
ogists who attacked the problem chiefly or solely from th ck
side would find the true solution. It required detailed paleo
tologic knowledge, particularly as to assemblages of fossils a -
their geographic distribution, before the faunal dintigetinad es
indicating separate provinces could be appreciated. Had Gan
geologists engaged on southern Appalachian problems received
a suggestion from the paleontologists of the striking dissimi-
larity marking the faunas pertaining to the lithologically — ‘]
equally dissimilar Ordovicie rocks lying respectively on the
east and west sides of the Great Valley, it is scarcely conceiy-
able that they would have failed to grasp the leading facts in —
the case. :

Excepting Walcott, who, however, confined his fruitful com-
parative studies to the Cambric, it appears that no paleontol-
ogist having sufficient knowledge of the Ordovicic faunas of the
interior, and accustomed to fit his biologic results to strati-
graphy, paid much attention to these problems.

tha ae wn steel Bye ase
a ee — = 6 ib c :

Pa
ead ‘9
2.

yi i

Se

. ’ *
° ‘
eae ss ee eee ee

*Geol. sur. Newfoundland. Rep’t 1864; also reprint in 1881, p. 47.

*This theory of Logan’s was brought to the attention of the authors
but a few weeks ago. Occurring as it does as a note appended to Mur-
ray’s report, it is not to be wondered that paleontologists remained in .
ignorance of its existence.

eC Pe however, was as yet undefined and hazy in its
ication, requiring much reading and field work to establish |
character, position and extent of the barrier that separated —
two basins or provinces. The paleontologic evidence in
| indicated a barrier of great length, dividing off from the
interior sea a long and narrow body of water in which sediments
wel e laid down containing remains of faunas having relations
to those pertaining to east Canadian and European deposits
2 than to those of the interior sea.
y _ American, Canadian and European -literature likely to bear
on the questions involved, made a pile so imposing that without
help the publication of the discovery must have been delayed
4 indefinitely, had the work been undertaken by a single person,
or it must have been brought out insufficiently supported by
_ facts to demand credence. Mr Schuchert therefore undertook
the labor of collating facts from published works, while Mr
- Ulrich continued the more congenial task of gathering additional
evidence in the southern Appalachian field. Between us then,
the evidence has been carefully weighed, discussed and corre-
lated, our original theories being constantly modified and
brought into accord with accruing facts till, finally, we enter-
tained sufficient confidence in the general truth of the proposi-
tion to submit the following summary of results.

woe ee re ee ee

The Appalachian series of folds, of which those only that sub-
_ sequently formed barriers, are discussed in this paper, probably
trace their origin to precambric times. Walcott,! we believe,

clearly demonstrated the existence of a long trough that dur- ek See

' 10U.S. geol. sur. Bul. 81. 1891.

_

St Lawrence
channel

been subjected toa slight ' vation, 1

itself manifest principally in Suncudead art
chian trough was almost drained of its sea, (
further to have been confined to the western half. of f the
trough by the emergence of a fold. > i 5
However, long before the close of the Middle Dar nbri |
present defined, a second period of subsidence set in, sul )
ence beginning along the east side of the Rocky mountain r'0-
taxis, and spreading northeastward. This submergen ich
might be appropriately called the St Croix invasion, x
important event in thedevelopment of the present contin n
being nothing less than the birth of the great interior con
tal sea, to which Walcott? has applied the term Mississ
This sea, sometimes almost oceanic in extent, vont rth
some interruptions and more frequent modifications of its out-
line, through all Paleozoic time. In Mesozoic time it was greatly 4
reduced and restricted practically to the Great Plains region.
With the beginning of the Upper Cambric, which, ian
ever, had been preceded by a period of partial reemergence :
and at least local erosion of the old Lower Cambric land, Bs
specially in the southwest, the new sea had transgressed —
beyond the Adirondacks and soon thereafter probably effected
communication with the Atlantic by way of the northern end of
the restricted Appalachian trough, or, as this portion might be —
more appropriately called, the St Lawrence channel? This —
communication with the Mississippian sea either continued
through the Upper Cambric and the following Beekmantown

+

age, or it was interrupted and revived again in the latter time. —
Only once thereafter, i. e. in the Utica age, did it serve the same

1 Am, ass’n ady. sci. Proc. June 1894. 42: 129-69,
?Mr Matthew finds this Dicellocephalus fauna common to America and
Europe. See Trans. Royal Soc, Canada, 1893, v. 10, § 4, p. 11.

y in isconsia: swliore't the Sepeaien were Sees the
per Cambric sea laid down great beds of limestone. These

siderable depth of water, which may explain the unusual paucity
is of animal remains contained in them, and 3) chemical precipita-
4 ~ tion as the main source of the matter composing them.
q As far as we can learn, it is only in the regions where Upper
_ Cambric deposits are decidedly arenaceous, as in New York, that
q ‘there is any marked distinction between them and the succeed-
ing strata of the Beekmantown age. Where they are made up
of limestones, like the Shenandoah and Knox formations of the
3 Appalachian valley, the Arbuckle limestone of Indian territory,
and the Pogonip limestone of Nevada, it appears that sedimenta-
tion and probably subsidence continued with little, if any,
marked interruption from practically the beginning of the Upper
Cambric to the close of the Beekmantown.
_ The close of the Beekmantown, however, marks the inaugura-

<
= Far

A oa

tion of a new arrangement in eastern North America. First, a
fold was developed nearly parallel with and presumably
a little within the western border of the original Lower
Cambric trough; second, another fold, that we have already
alluded to as having emerged early in Middle Cambric time,
and that was now only accentuated, and reemerged, arose
along a line marked in the south by the present western out-
line of the Ocoee series of rocks and in the north by the Green
mountains of Vermont. Though these folds extended appar-
ently without serious interruption from Alabama to and far
beyond Quebec, it is doubtful whether the trough bounded by
them was ever again entirely submerged subsequent to Beekman-
town time. Between them, the western one in the southern and

| ; moteness from steep shores of the areas receiving them, 2) con-

UpperCambric
limestone

Beekmantown
limestone

Era of folding

ei ests Leu ante e

A achian
valley trough

"The western of these two folds, wtin3 aS
indicated on the accompanying map, Pe,
ian valley barrier or fold, while the eastern in called t
barrier or fold, when we refer to the middle po: and |
end of the uplift, and the Green mountains barrier in speakin
its northern end. 7a a eg

Coincident with the emergence of these folds, the Missi sip
pian sea was restricted to narrower limits, but at pres on
not safe to indicate the extent of the land areas then form
Still it seems certain that, with the exception of mate Ok a ig
basin and Levis channel defined in the following paragraphs, all
of New York was above sea level. ee. +

The space between the two folds we shall refer to g e n-
erally as the Appalachian valley trough or simply Vall
trough, and, in order to facilitate reference and geographic —
accuracy, it is divided into three unequal parts. The 4
southern third, extending from Alabama to southwestern Vir
ginia, we shall refer to as the Lenoir basin, the middle third,
extending on to New Jersey, forms part of the subsequent Cum-
berland basin, and the northern third, extending as far as New- |
foundland, will be called the Levis channel. Parallel with, but
shorter than the Levis channel, and immediately northwest of
the Appalachian valley barrier, lies the Chazy basin, with its
typical Chazy deposits and fauna. :

As will be seen later, these divisions are distinct though in-

a
“10: na

definitely bounded basins, of which the central one was com-
monly occupied by the Mississippian sea, while the terminal
basins were generally taken up by Atlantic waters.

Immediately following the emergence of the folds and the
broader land area just mentioned, there began a period of sub-

of FE ae ee

nines me re continued, re hat serious in- ee
yn, to the close of the Black river, when elevation, result-

fhe first emergence and subsequent erosion of the Cine
1n and Nashville domes or parma of Suess, took place. In-
C ‘meantime, the Mississippian sea, which seems to have

ching the Mohawk and St Lawrence valleys, as we shall have
ess to explain more fully, just before the close of the Stones

With the earlier part of this subsidence, the Atlantic ayedea
the continent westward by means of the two subparallel and
- closely approximated channels that we have called the Chazy See eae
bay and the Levis channel. The former extended along the
= northwestern side of the Quebec barrier, which separated the

_ two channels, up the St Lawrence to the northeast angle of the
Adirondack mass, where it divided, one arm entering the Ottawa
basin, the other passing on up the Champlain valley to or about
Westhaven. The typical Chazy formation, which represents the
deposits of this bay, bears evidence in its members of having
encroached southward and westward in the arms, the latest beds,
except where, apparently, they were removed before being —
covered by the next formation, extending farthest south and_
west.

i oak De

. The Levis channel, which occupied the narrow trough between Levis channel
: the Quebec and Green mountains barriers, extended from New-
foundland southwestward as far at least as Rensselaer county,
N. Y., where Ruedemann has found the typical Levis fauna. Its
deposits consist almost wholly of shales, with occasional rather
local thin bands of impure limestone and accumulations of con-
glomerates, as at Levis opposite Quebec city. The faunas, which
in their- general aspect are decidedly European, consist mainly
of graptolites, that of the Levis formation being particularly

characterized by several species of Phyllograptus. The respec-
/

Normans kill
shale

Path: ‘the. Tach channel as. oeaiee ained. T
ence continued in the Chazy basin till Bi ack ri
but, if the drainage occurred simultaneously oe |
nels, appears to have been of briefer duration in
channel. On the other hand, it seems very ‘likely
the Chazy bay was emptied sometime in advance of t he.
channel, allowing deposition in the latter of beds holding :
lower Dicellograptus and Agnostus, Ampyx, Aegina and P at
rula fauna, which is common to Europe and the Levis ch ni} Bes
The earlier emergence of the Chazy channel is rendered v very
plausible if we assume a period of compression at the close o
Chazy, causing the strata in the western channel to be pus bee wi
on the sloping Adirondack and Laurentian masses beneath them,
and high enough to empty the western channel but not the Levis
channel. The same assumption would explain the icveloae
of-the supposed barrier, referred to a page or two farther on, |
across the mouth of the Ottawa arm of the Chazy bay, whieh,
if it ever existed, must have arisen about this time. ee as
The deposits and fauna of the supposed lower Dicellograptus —
zone in the Levis channel are now known chiefly, if not solely, 7
from limestone pebbles and boulders preserved in the conglom- —
eratic horizon at the base of the Normans kill shale, the bed
itself possibly being now entirely covered by overthrust Cambric
rocks. The fauna contained in these pebbles, «s worked out by
Ruedemann,' contains species indicating some communication
with the Mississippian sea in the vicinity of Albany N. Y.; or it
may be that the sea of the Normans kill shale, which trans-
gressed farther westward, also washed surfaces laid down by
lack river and early Trenton seas. :
The Normans kill shale, which, as we have just said, trans-
gressed a little farther west, also extended farther southward

*N. Y. state mus. Bul. 42. 1901; Bul. 49, 1902. p. 89-94.

ning, we see that the Chazy of the Champlain-Quebec val-
and the Ottawa basin was succeeded by an interval of eleva-
n and probable erosion preceding the Black river invasion.
PE ixpoin: we conclude, the upper limit being fixed by evidence ~
4 ouched on in a succeeding paragraph, that the Normans kill
shale is about Middle Trenton, as demonstrated by Ruedemann, é

3 a a little later in age.

While ‘the Chazy and the greater part of the Stones |
river deposits were being laid down elsewhere, nearly all of eam
the middle Appalachian area, together with New York and
much of Canada north of the St Lawrence, constituted a great
and continuous land area, and it was only with the advent

$f the Black river and the underlying Lowville limestone, which
is equivalent to the extreme top of the Stones river, that the
_ Mississippian sea at last spread over a considerable part of this
4 territory. Judging from the uniform age of the basal member piack river

invasion

2 of the Mohawkian in New York and Canada, it seems almost
3 certain that the Black river sea accomplished the submergence
7 of the troughs surrounding the Adirondacks and lying south of
- the Laurentian nucleus, or Canadian shield of Suess, almost
: simultaneously. It is therefore eminently proper to speak of this
_ ‘Stage of the subsidence as the Black river invasion. ,
2 The Trenton sea seems to have maintained very nearly the

3 _ Same outline here as the Black river, and like that sea, at first,

and then again near the close of its age, transgressed the Quebec

4 *Weller. Geol. sur. N. J. An. rep’t, 1900. p.5; and Kiimmel, p. 53.

=-

Ottawa bay

Utica invasion

intervened, its western eats appi nine the

turn covered by the second. The latte ‘tward rd tr
of the Trenton is indicated chiefly by thetaaieal
shale overlying the Normans kill. A careful study of
mann’s list of this fauna reveals stcise incompati _
late Trenton correlation. z
Immediately succeeding the Chazy, there is reason t
a fold was developed across the mouth of aed
bay that has since been worn down to Upper hs an = |
rocks. This fold must have been higher than the land f yrmer]
bounding the western end of the bay and senate
Ottawa bay now coming in from the west, probably by * ‘
Lake Nipissing, from the narrow Champlain-Quebec basin. 1 s
separation is indicated by both structural and paleoniie y o
evidence. oer.
At the close of the Trenton the Cincinnati axis or parma
experienced one of its periodic uplifts, and with it much i
the area west of it was raised above sea level. The region to F,
the east of it and north of the Ohio river, on the contrary, seems — &
to have been slightly depressed. Apparently the subsidence
was greatest in the Mohawk valley and in the Levis
basin of the Appalachian valley trough, and sufficient to
render the Quebec barrier wholly ineffective here. The north- 7
east communication with the Atlantic, now considerably |
enlarged by the subsidence, brought in with the decided south- }
west current, ingeniously demonstrated by Ruedemann,! a fauna .
wholly new to the Mississippian sea, having, as has been
already asserted by Matthew and more recently by Ruedemann,?

>
strong European affinities. 2.

Am. aan 1897. 19:367-91; 1898. 21:75-81.
*N. Y. state mus. Bul. 42. 1901. p. 562.

“7 =".

ati itself t6 any sesh eens in the
: of succeeding aes of the eee sea. ae ;

se =

the Frankfort shales, which we regard as equivalent a ;
Middle aac i a rae of peel Ss Cincinnati Bute sy

| Traine of the Hudson river valley has been shown ae Rucacnnn

& to be the equivalent of the Frankfort shales with a fauna transi-

« tional from the Utica to the higher Lorraine.
In the north the effect of the lateral compression to which the

_ Appalachian region was periodically subjected during the Pale-

_ 020i¢c is particularly marked in the area lying just east of the

_ Adirondack mountains. The Ordovician sediments here were yaximum of
"piled i in distorted and broken masses and largely covered by over- east of Adi-
- thrust Cambric deposits. As might be expected, the eastern one

: _ of the two (Chazy and Levis) channels that intervened between

P the Adirondacks and the Green mountains has been almost ob-

_ literated, So that it is now very difficult to trace out the relations

of the remnants of its deposits, which crop out only here and

E there from beneath the overthrust masses of older rocks. Still,

with careful stratigraphic and paleontologic comparison, we

believe the task is not hopeless. Ruedemann’s important results

about Albany, Ami’s recent work at Quebec, and Dale’s careful
areal work, look, to say the least, encouraging and augur even

‘ greater results in the near future.

eae ae ba - int is

*Cincinnati soc. nat. hist. Jour- 1902. 20:49-100.

2

ro Sa ee seiei yey

Rome barrier
and Lenoir
basin

; Athens and
Knoxville
troughs

Correlation
of Ordovicic
deposits in
Lenoir basin

ee ?. fe a

[ald donee ia the bedi sa? eels g dire ect e¢
with the north Atlantic, another etter: tks.
deposition in a bay separated from the } sin a ite pil n
Rome barrier, which is the sharply defined southe mn ex
the Appalachian valley fold. This bay may take th
Lenoir. It communicated with the Atlantic at its s
and extended northeastward between the Rome and | Chill
barriers from middle-eastern Alabama to southwester

The Lenoir bay occupied a, synclinorium contain in
disconnected longitudinal folds high enough to affect t
tion of currents and consequently the character of the s
and, in a smaller degree, faunal distribution. In a general ¥
the deposits may be divided into an eastern (Athens y erin
and a western series (Knorville trough), the men pe coat
which, on account of differential warping and subside oN
and lateral conjunction, overlap or grade into each « ; meno
along the shifting median line. On the eastern side w x
have the Athens shale and sandstone, which are supposed |
to correspond with the Lenoir limestone of Safford — eis
part the same as the Chickamauga limestone of Haye
Campbell and Keith), and its great lenses of Holston marble
occupying the western half. Compared with the sediments in
the northern Appalachian troughs (Chazy basin and Levis—
channel), they probably fill the interval there occupied by the
Chazy, Levis and Normans kill shale, The Tellico sandstone and
the Moccasin limestone follow, the former in the eastern half,
the latter in the western, while the Sevier shale spreads over.
both sides. The last formation probably is equivalent in time ~
to late Trenton and, possibly, Utica.

These Lenoir bay deposits contain faunas wholly distinet from
those pertaining to the true Chickamauga limestone series, which

- ay

“confines of the Lenoir bay. The result of this revolution and

invasion is the Bays and Clinch sandstones, and the lower, non- Bays and
; inch inva-

sion

_ ferruginous, shale division of the Rockwood. formation, all of
which, as is indicated by fossils collected from the last by M. R.
_ Campbell, of the U. S. geological survey, are of Cincinnatian
_ (perhaps Lorraine) age. Continued elevation of the southern
_ end of the Valley trough is indicated by the fact that of the three
_ formations mentioned the first extends farthest south, the sec-
ond not so far, and the third again falling short of the Clinch.
Before the close of the Ordovicic both the Lenoir bay and the Simone
_ Cumberland basin had been raised above sea level. This emer-
; gence took place about the beginning of the Richmond age, dur-
a ing which the Mississippian sea was restricted to the Ohio valley
: — and west and south of the Cincinnati line of uplift. Prior to
this time, or at the beginning of the Lorraine, which probably

=?
2
:

corresponds very nearly to the time of the Bays and Clinch in-
yasion described in the preceding paragraph, there was another

.*

E.
emergence that reduced the Frankfort phase of the Mississippian
sea by excluding its waters from the valley of the upper Missis-
‘sippi and from the various basins lying east and south of Rome

N. Y. We see, then, that both of these emergences were ac-

hp Pee et ie,

:
rr BS a

Ere SE Ore tee
"¥

Taconic
revolution

bearing on the point indicating ope

Mississippian sea, then existing, with An
Europe. But as this communication wits tair
of the St Lawrence-Champlain valley, and ar »
is not intimately connected with the subjects of hi by
discussion is deferred. , Be
Toward the close of Ordovicic time the lands : 1 sea:
evidenced by the two Lorraine and icheneat ¥ om or
and submergences described, had become uni table ple
followed one of the greatest earth pulsations it
American Paleozoic history. The disturbance referred 1
Dana! says gave birth to the Taconic mountains; and w e
therefore call it the Taconic revolution. That this mc ver mi
was one not only of elevation but also of considerable fe ding
of the earth’s crust, is shown in the fact that the Heldert a ,
deposits overlie unconformably the Ordovicie strata, asa
Becraft mountain, New York. That its effects were exter .
is indicated by Dana’s remark, “The Taconic... ccna 0
upturnings appear .. . to extend all the way from the St Low.
rence valley to New York city.” asic
This revolution affected all North America, and there was
land perhaps throughout from Richmond to Oneida time. The |
length of this land interval we can not perhaps now ascertain
satisfactorily, because there are no Mississippi sea deposits by
which its duration may be measured. In Minnesota, and more —
particularly in Manitoba, there are late Ordovicic deposits with
prophetic Siluric genera and species which apparently indicate
that the land interval was not of long duration. “After a moun-

5

tain birth,” says Dana,’ “ there has commonly succeeded a time —

*Manual of geology. Ed. 4. 1896. p. 386 and 531.
7Manual of geology. Ed. 4. 1896. p. 386.

i Pe eae se Pot,
‘Dp pressure and then occurred adjustment

: pushers this i is true in this. instance, | ::
it continued nearly

z . Osw ’
vegan pabaideace or invasion, as it may be called, te Senses os

: the Oneida, and continued with little interruption to es

er, So that in the region south of the Mohawk river the Euryp-
us bearing Waterlime, which is the uppermost division of the
lina, appears not to have reached the eastern side of the
lderberg mountains. The Clinton, Niagara and Salina also
ch out one after another west of the Helderberg mountains.
oa 0 the south, the equivalent deposits transgress even less toward
3 the Appalachian protaxis, the eastern line in middle Pennsyl-
. -vyania Swinging westward to the vicinity of Altoona. From
- this point southwestward the line, judging from the data
4 available, seems to have run about parallel with the general
_ trend of the Appalachian folds into West Virginia, and it prob-
; - ably swung eastward again toward the Appalachian valley fold
before passing through that state. This westwardly bent
_ line has great significance, because it corresponds with the course
of a barrier defining the western limit of another basin, the
x Cumberland basin, that was occupied by an Appalachian Cumberland
a Mediterranean, with a fauna very different from that of oa oder
_ the contemporaneous Mississippian sea. We mention this
a little out of the regular order of our description, so that the
reader may understand why the Siluric deposits east of the
4 Helderbergian barrier just located are not regarded as con-
‘tinuations of the sediments of the Mississippian sea.
In the southeastern portion of the Mississippian sea the Oswe-

‘gan invasion was limited by the Rome barrier, and began with nag oie
a shale instead of conglomerate and sandstone. This character
of deposits continued with occasional interruptions of thin, fer-

ruginous, fossil limestones, and locally heavier beds of sand-

Stone, to the close of the Clinton. There are no deposits of

‘\

ea Fe) a Pe

Ccew a
a

=_

Cayugan
emergence

Helderbergian
invasion

Niagara to the midate Devenie: phe | ‘incinnat

above sea level at the same time, and-
Tennessee land in such a manner that a broad
between the two domes. Neither of the latter was ey
entirely by Siluric strata, these being laid down o:
gently sloping shores and in embayments ene
warping of their surfaces. The succession of th > de:
these embayments shows very clearly that. thee) ot 1 i
the close of the Clinton was soon checked, and tha
subsidence prevailed in later Niagara time. ia

Throughout Cayugan time, on the contrary, the Mis i
sea was growing shallower, the floor of the sea having
almost gradually till, at the close of the Rondout, the ) y
interior of the continent west of the Helderbergian ee ad
become land. This important emergence, for which we DOPE ose
the name Cayugan, continued from Waterlime to Onondaga time e,
when the Mississippian sea again came in from the suthvet
spreading far and wide in the United States. In its eastw |
progression this invasion (Onondaga) did not reach middle and _
east Tennessee till near the close of the Black shale, which i
commonly correlated with the Genesee. The southern Black
Chattanooga shale, however, may really represent late Devonic

time only, since in complete sections the shale in question seems
to pass very gradually into undoubted basal Mississippian (Car-
bonic) shales. ce

While both the Oswegan subsidence and the following Cayu-
gan emergence were affecting the area to the west of the Helde

REPORT OF THE STATE PALEONTOLOGIST 1901 649

at pergian barrier, mentioned above, the region east of the barrier,
@ comprising the Cumberland basin, was steadily going down, the
a ‘subsidence allowing an invasion of an Atlantic sea and fauna
© to which the name Helderbergian invasion may be very appro-
priately given.

This invasion brought in a European fauna by way of the
Hercynian chain believed to have connected North America with
eentral Europe (Bohemia, Hartz, etc.). We think this line is
in the main correctly drawn by Bertrand,’ though we would

draw it on the American side more to the north—nearer to his

é
]
i
;

kanian deposits of Gaspé, Quebec, into more direct connection
with those of the Appalachian Mediterranean.

This invasion of the United States began early in Siluric time,
occupying then and to close of Oriskany time the growing Cum-
berland basin lying, as described above, east of the Helderberg-
jan barrier. The connection between this Appalachian Medi-
terranean and the Atlantic, which will be further discussed in
treating of the Marcellus invasion and the Skunnemunk trough,
is supposed to have been about in the region of Chesapeake bay.

To the north and south of Cumberland Md., there is a great
series of rocks, beginning with shales and passing upward into
limestone, and characterized by a succession of prolific faunas.”
Very few of the species of these faunas are identical with species
of the Mississippian sea of Siluric time. The earliest fauna
recalls the Clinton, and passes into one which may be compared
with the Niagaran, and then a great series of limestones,
abounding in minute Ostracoda, which may be compared with
the Salina on account of the prevalence here also of larger
Ostracoda of the genus Leperditia. Then comes in without

*Soc. geol. de France. Bul. Ser. 3. 1887. 15:442.

*This series of rocks rests on the Tuscarora and Juniata formations.
These coarse deposits have afforded very little satisfactory fossil evidence,
So that we do not yet know whether they belong to the Mississippian sea
or the Appalachian Mediterranean.

Caledonian chain—so as to bring the Helderbergian and Oris-

Appalachian
Mediterra-
nean, or
Cumberland
basin

t Cun a | berlar nd and

dieting: pas causes aaa i Y
after another till, finally, only a little of the Teld
Oriskanian series is represented in the Sneedvi
limestone of southwestern Virginia and northeaste
Northward from Cumberland, through Pennsylvania
Jersey into New York, the lower formations ae i
same manner as in the south, so that in the Kittatir ny a

of New Jersey it is practically the Decker Ferry fo — ‘ion >
that rests on the “red and white Medina” or Sha vangu
From here north, however, the Decker Ferry, Maniiagl nd ies 1-
derberg formations continue in full force to near the Mo aa
river, presenting thus a condition differing widely from that
obtaining in the southern end of the basin. It is in this north-
ern area that one finds the extensive and readily access ble-
Helderbergian deposits that furnished the fauna so well de-
scribed and beautifully illustrated by Hall. For this reason,
and because the subsidence appears to have been continuous, —
we have chosen the name Helderbergian for the invasion. In the 7
other cases of movements named by us, we have taken the name ‘

* Geol. sur. of New Jersey for 1899. 1900. p. 7-21. Some of these identi-
fications are admittedly provisional and require verification, Mr Weller
having followed Hall's correlation of the Coralline limestone as the eastern —
representative of the western Niagara, an obvious error now that we know ~
that the Coralline limestone lies just below the Rondout, at Rondout N. Y. —
However, the typical Rondout should not be confounded with the Water-
lime of Buffalo N. Y. The Rondout formation is but the base of the Man-
lius, and the former is completely transitional downward into the Coral- —
line limestone, The Helderbergian invasion in New York begins with the ~
Coralline, while the Cayugan emergence closes with the so called “ Clin-
ton’”’ of the Schoharie section, which we consider the overlapping eastern
edge of the Salina deposits, and certainly not equivalent to the true
Clinton.

a.”
~4

of Helderbergian and Oriskanian, whose faunas are closely
| lated to those of their equivalents in New York; and another
area occurs near Dalhousie N. B., with a fauna peculiar to it.
¢ oncerning these two areas, the latter appears to belong to a
subprovince distinct from that of the ie caaiees Mediter-
ranean,
_ The Helderbergian invasion of the southern Mississippi valley
a Fecgan after the Cayugan emergence, since its first deposit seems
to be of Coeymans age. Part of the underlying Meniscus or
_ ©lifton limestone of Safford may also belong to this invasion.
It came in from the south and spread north along the western
side of the Cincinnati arch through Tennessee into southern
illinois and Missouri. The invasion continued throughout Hel-
_ derbergian time and ceased with the Camden chert of early
Oriskany age. Another area lies in Indian Territory, and the
faunas of all the southern Helderbergian and Oriskanian depos-
its are of the Appalachian facies.

No Helderbergian deposits are reported from the Rocky moun-
tain region, but we have good reasons for stating that equiva-
lent deposits occur in the Devonic of the White Pine and Eureka

_ districts of Nevada as defined by Walcott and Hague, holding a
rather peculiar, though on the whole recognizably Helderbergian
fauna.

The Oriskany formation in the Appalachian Mediterranean,
or Cumberland basin is in full force only in the region to the

| north and south of Cumberland Md. In southern Pennsylvania,

a

~ Pare se oe ee » e

*Schuchert. Am, geol. 1901. 27:245-53.
* Manual of geol. Ed. 4. 1896. p. 558.

Pe

to be the case. About Gaspé there is a grand develop- |

Oriskanian
emergence of
Appalachian
Mediterra-
nean

Saind.,. berland basin, there still remained in southern Rowe ‘ for ka

plan: but in eastern ie Werk: it sone to.
portion only that is present. With Lower ( Ori ‘isk
southern extremity, and Upper Oriskany oxy Hi int :
end, the movements evidently were directly opposite a: at
extremities of the Cumberland basin during Oriska init ian n z |
The land conditions that succeeded the Oriskany i in
land basin continued till about Marcellus or M o -
time, when the later Devonic deposits of the Skunne .n
sion were laid down.

Immediately succeeding the Oriskany emergence of t

depression through which the Atlantic fauna of the Ori
invaded the Mississippian province. This invasion, coming i Ke
from the southeast (the Esopus, which is only a phase of the
Oriskany, is 700 feet thick, according to Ries,’ in Orange county 3
N. Y.) spread northward, over the Oriskany, and, after cros
the Helderbergian barrier at Rome, continued on weateal Ae
way of Buffalo, where remnants of it are seen in the cement
quarries.” Finally, the last of this deposit is seen near Cayuga —
Ont. i.e.

The Oriskanian invasion attained the last locality about the
Same time that the Onondaga invasion, coming in from the
southwest, arrived there, the result being that the Onondaga —
and late Oriskany faunas, originally very dissimilar in character,
became one, making together what is now known as the eastern
Onondaga fauna. “a

‘Ries. N. Y. eiateed 15th an. rep’t 189 1898. 1:402.
*Grabau. Geol. soc, Am. Bul. 1900. 11:5 5-62.

Siti

REPORT OF THE STATE PALEONTOLOGIST 1901 653.

ui The blending of these two different faunas can be seen to best
E- advantage in the townships of Oneida and North Cayuga, Ont.,
- where there is a sandstone filled with late Oriskany fossils.
_ The sandstone rapidly passes into a sandy limestone and then
_ into the typical Onondaga limestone. If it were not for the
_ structural dissimilarity of the beds, these two faunas could not
be separated, since it has been shown that out of 71 species
found here, not less than 42 pass up from the lower horizon
into the Onondaga;' yet the lower horizon has such characteristic
Oriskany species asSpirifer arenosus, Chonostro-
phia complanata, Rhipidomella musculosa,
Stropheodonta magniventra, S.vascularia,
Eatonia peculiaris, ete. On account of the marked
Onondaga aspect of its fauna, it is unwise to call this Ontario
deposit Oriskany any longer, and we here propose to call it the
Decewville formation, taking the name from the village nearest

_—_ Tee ote we

to its exposures. We include in the formation the coarse basal
sandstone and the thin bedded sandy limestones up to where
the typical Onondaga limestone appears.

A careful analysis of the Schoharie grit fauna of eastern New
York, and of the Pendleton sandstone of Indiana? will probably
also show a blending of the invading Oriskany and Onondaga
faunas, though probably less marked than it is at Decewville
Ont.

A further instance, or rather, a survival of the blending of the
Oriskany and Onondaga faunas, is shown at Clarence Hollow
N.Y., where Spirifer arenosus (describedasS. unica
Hall) occurs in the Onondaga limestone.

By the time the Onondaga invasion had become established
in the Mississippian province, the Cumberland basin, including
its last remnant, the Oriskanian channel already discussed, had
been wholly emerged, thus cutting off all communication with
the Atlantic in this region. This severance, however, was of

*Schuchert. N. Y. state geol. 8th an. rep’t. 1889. p. 51-54. Also Geol.
soc. Am. Bul. 1900. 11:323-26.
*Siebenthal. Ind, dep’t geol. and nat. res. 25th an. rep’t. 1901. p. 347.

See iy ce a oe
(ab ec ntime aff e.%

eae foathat the con acd ee
7 ~U “ _ a” ve La
om Nigekeae eit nee ‘a ae. me
ia aA "+70 | aM ? 4 iS wba a 3 oe i a ee

a, be begs 7

ie “Atlantic: nid: Miesimeioolas Sas eel
down in the modified but Rete a Ot —
In the Skunnemunk and Green Pond mountain
former in southeastern New York, the latter: ie ve"
there is a series of coarse deposits apparently oce " ying
cline. The oldest formation above the oicueea lepos
the Green Pond conglomerate, supposed to be of thang
Shawangunk farther north. From this on, deposition ap}
to have been continuous to the close of the Heldert nei an, V
this area, in common with the Cumberland basin to the west
it, was affected by the elevation of the eastern side of the one
tinent. Resubmergence began here with the Monroe s eS, hi
which rest on Oriskanian strata, and continued cae a rT we

eenunk Bellvale flags into the Skunnemunk conglomerate, which Dartor j
nis suggests “ may represent the Oneonta” or “ the formation may

be the equivalent of the coarse beds of the Chemung.” Fossils _
from the Monroe shales sent by Darton to Hall were pronounced —
by the latter to be of “ typical lower Hamilton (group) specie
The Bellvale flags contain Tropidoleptus carinatus, —
Spirifer mucronatus, and, more commonly, land —
plants, recalling those described by Dawson from the Gaspé ;
sandstones. According to Ries the total thickness of the De- —
vonic deposits (succeeding the Esopus or Oriskany) in the 4
Skunnemunk and Bellvale mountains of New York, is about 1500
feet; while Darton gives a thickness of 5400 feet for the equiva-

lent series in the Green Pond area of New Jersey. This differ-
ence in volume is cited in support of our opinion that the great-

‘Darton. Geol. soc. Am. 1894. y.5; Ries. N. Y. state geol. 15th an
rep’t 1897. 1898. 1:408-4, 410-24.
*Darton, op. cit, p. 375.

- aspects from those of the Devonic west of the Cincin-
axis. The porte Naa eat between these basins or ons

a We tors further that it was ‘nina net these channels s

- that the Skunnemunk trough and the eastern Mississippian sea,

— York at the time, received its Marcellus accessions. These
- migrants are now found mixed together with the indigenous
_ early Hamilton faunas as far west as western Ontario (Thed-
ford). Some of these European accessions are Strophalosia,
Liorhynchus, Tropidoleptus, Tentaculites, Styliolina, Actinop-
_ teria, Pterochaenia, Bactrites and Tornoceras.)
Our derivation of this fauna from Europe by way of the Atlan-
tic goes further than Dr Clarke’s views. He regards it “as an
_ invader from the southeast along the inner or Appalachian face
F of the interior sea.”? The Marcellus is well developed about
- Cumberland Md., and south to about central Virginia, where this
_ formation pinches out. We therefore conclude that the invasion
q from the Atlantic was somewhere in the Chesapeake bay region.
The bulk of the Marcellus fauna is however indigenous to the
eastern Mississippian sea and is a development out of the

Onondaga. —
Iran ae ae eS ee
1We should not have been able to make these statements, had we not
the excellent work of Dr Clarke on the Marcellus faunas. These papers
are the following: N. Y. state geol. 4th an. rep’t 1884. 1885. p. 11; N. Y.
state mus. 42d an. rep’t. 1889. p. 406-97; N. Y. state mus. Bul. 49. 1902.
p. 115-38 and Miss Wood’s paper following on p. 139-81.
Pap. p. 115.

Error ee Poe LG Le Oe ne ee ae
\

re of 7e Dhdlichion valley trough, and hold, as do also ye
valent sediments of the Cumberland basin, faunas having

- the latter covering Virginia, Maryland, Pennsylvania and New

: <¥

=

Ac RSE,

MIEN Reade

ent
ete A

work, consists of no less Shi eight. genera 25°
yet in no other American area holding beds of § Similar P
more than one species of goniatite. (Manticoce
mescens, the widely dispersed European sp Be , is
found in Iowa and on Hay river, latitude 60° no t] h.)
fauna is closely related to that “of Martenberg in Wes Mi |
How long this Atlantic invasion continued we do not ] et . atti
state, but it is certain that the indigenous Upper Devonie ft
of New York not only received the above ipsa ;
migrants, but also some from Iowa, as in the High ches
faunula. The Mackenzie basin Upper Devonic fauna, ¢
terized by Stringocephalus burtini, is ofa é in
subprovince; but the geographic derivation of that fauna we e ¢
not yet know. We are however satisfied these Macl
Devonie deposits had no direct connection with those ~ mc :

2 eats AS :

Carbonic ‘le A

There appears to be a complete series of Devonie deposits, —
with the possible exception of the Onondaga, in the middle third —
of the Appalachian Valley trough, but early Mississippian seems ;
to be wanting in this portion. In the southern end, the early
Carbonic, represented just west of the Rome barrier by the
Fort Payne chert, also was partially excluded; but the St Louis,
and possibly Chester, are represented in the trough at several
paintn. The Fort Payne chert is represented within the extreme

‘Am. geol. 1891. p. 86-105; N. Y. state geol. 15th an. rep’t. 1898.
Pp. 51-81; also ib. 16th rep’t, extract. 1898. p. 31-143.

*Clarke. p. 136.

*For this section Mr Ulrich alone is responsible.

sien rales synclinorium. Phpee cui depres- —

ns. may in a general way be said to have been occupied at an

‘lier period by the sea which laid down the Devonic Black

ale, and which entered the trough probably through the same

| opening. Subsidence of the middle third of the Valley trough

S continued in second half of Mississippian time, resulting in, : 7
greater expanse in the Appalachian region of Newman limestone
and Pennington shale, which, together, represent the St Louis
and Chester deposits of the Mississippi valley. These forma-
4 tions, however, do not extend over much of the basinlike area
~ occupied by the early Mississippian- “Waverly sea in Ohio, north-
east Kentucky and the adjoining corner of West Virginia, the
Waverly basin, lying between the middle Tennessee-Cincinnati
_ line of uplift and the Appalachian-Chilhowee barrier, having
been in St Louis and Chester times, much reduced in its northern
and northwestern extent.

”

.
i
“a

_ The Carbonic strata of Michigan were deposited in a basin
formed by the bifurcation of the Cincinnati axis, and probably
had only a slender or possibly no direct connection with the
Waverly basin to the southeast of it. At any rate, the evidence
- in hand indicates that, if the connection existed at all, it was
Severed about the beginning of the St Louis age.
4 The coal measures east of the Mississippi river were inaugu-
_ rated by a slight subsidence beginning perhaps with an ice age.

pitied ‘.

a

ward continuation of the are eee
there was a shallow basin that, ‘a eet ioe en:
’ occupied by a bay. This bay was in existence ari g
or a portion of the time consumed by the dep - |
Pottsville series, and, as it became filled up y ‘

subsidence continued, gradually aoe into the ma
A io ES .

Ses a aneeteen amt ante eel

See |
Oriskanian

> Helderbergian

Longwood

Green Pond
Land

Land

<- Probably land->

GEORGIA

Se

- Becraft

Marvollos
Onondaga |

Schoharie

Decewville and bgecei
Upper Oriskany

Lower Oriskany :
Kingston |

New Scotland
Coeymans
Manlius
Decker Ferry
Rondout
Salina
Guelph
Lockport
Rochester
Clinton
Medina
Oneida
Land
Richmond

Lorraine
Frankfort

UTICA

Upper Trenton
Normanskill
Lower Trenton
Black river
Lowville
Stones river and Chazy
BEEKMANTOWN
POTSDAM

Lower St Croix
GEORGIA
VERMONT

Unclassified time scale for eastern North America, and correlation of formations and land intervals in the Mississippian, Appalachian valley, and
Atlantic provinces, and their respective basins

The same name in two or more columns Indicates direct marine and faunal connection elther before or after the birth of the basin under which it Is listed. Different names on the same line indicate supposed equivalence in age only.

Names of formations deposited in the Mississippian sea are printed in ordinary type, those laid down in Atlantic waters in italics, while names of those deposited when the Mississippian
and Atlantic seas were in communication by way of the St Lawrence channel] are printed in SMALL CAPITALS, and heavy face type is used for formations deposited in Atlantic waters
that entered the territory of the Mississippian province by way of the Cumberland basin.

MISSISSIPPIAN
PROVINCE

APPALACHIAN PROVINCE

ATLANTIC PROVINCE

Mississippian sea

Chazy basin

APPALACHIAN YALLEY TROUGH

LENOIR BASIN

Cumberland basin

Skunnemunk basin

GENERALIZED TIME SCALE FOR
EASTERN NORTH AMERICA

Levis channel Middle third
Knoxville trough Athens trough
Carbonic Land Carbonie Carbonie Carbonic Carbonie Carbonic Land Carbonic
Chemung } ° Chemung ) } Chemung Skunnemunk Chemung
Portage ails Portage | | Portage Portage
Genesee. aa ?Chattanooga | }Chattanooga \ Bellvale Genesee
Tully . 22 * Hamilton f | Hamilton Tully
Hamilton ) Land So J J i Monroe Hamilton
Marcellus Deposits not well ae Marcellus Land Land Marcellus Marcellus
Onondaga known tate A | Land in south } Onondaga
{ ie S Onondaga in north > Land
Schoharie Land ( S| Schoharie J Schoharie
Decewville as Land Land Esopus — Esopus Decewville and Esopus
Upper Oriskany | qa Trog mountain I'vog mountain Upper Oriskany Ouelkonian | Upper Oriskany
Land Land ® 2 Land Land Lower Oriskany ) | Lower Oriskany
U 5 a Kingston | Kingston
St Helens island 22 Beoraft \ Pe Becraft
Land a. New Scotland Sa BATE New Scotland
Land cS Coeymans } | Coeymans
Manlius in part Land a Manlius | Manlius
Land oq ) ? Land | Decker Ferry
Rondout aa +} Formations at Pinto Md.) {° ~ | Rondout
Salina Land BQ J J Salina
Guelph ) Ne | , ) Guelph
Lockport | 8s {Noname. Formations at \ Longwood Loekport
Rochester { SE pees a Cumberland Md. Rochester
Clinton Anticosti series | | Clinton
Medina j t Tuscarora and Juniata t Green Pond eae
and Land ' Land Land Land
Richmond Anticosti Hudson Lower Rockwood Richmond
river V Clinch
Lorraine Land Land Land Bays Land Lorraine
Frankfort Frankfort Frankfort Frankfort Land Land A A Frankfort
UTICA UTICA UTICA UTICA ) d | f UTICA
) Upper Trentor ) | ( Sevier ) | { Sevier 'g Upper a tanton
Trenton Trenton Normans kill Trenton | | —_— 3B Normanski
Lower Trenton 4 Moceasin Tellico cit oo = Lower Trenton
Black river Black river Black river Black river | SAC o i Black ay er
Lowvyille Lowville Part of time land | Lowyille | Lenoir J | (Athens ~ Be 3 Lowville 1 Chaz
Stones river Chazy Levis Land J ones 8 ° Stones river and Chazy
BEEKMANTOWN BEERKMANTOWN BEEKMANTOWN BEEKMANTOWN | BEEKMANTOWN | BEEKMANTOWN Deets Ay BEEKMANTOWN
POTSDAM POTSDAM Land POTSDAM POTSDAM POTSDAM Cs y POTSDAM aoe
Lower St Croix Land Middle Cambrie Middle Cambrie | Middle Cambric} Middle Cambric Lower St Croix
Land | GEORGIA GEORGIA GEORGIA GEORGIA V GEORGIA GEORGIA
Land Land VERMONT VERMONT VERMONT VERMONT VERMONT

— &

as

.
»

ees

=

ons -
+s « =
_— -
2 . ad —_ %

ie —

sea on the Canadian shield attained considerable extent on
4 1e north and west and more particularly on the south. The
east shore, on the contrary, remained nearly the same till com-
pe d ratively recent time—probably Postcretaceous.

The present main lines of elevation of the continent were in
- existence in Algonkian time and have been maintained without -
serious modification to the present day. Concerning the anti-
.- - clinal folds that began in Paleozoic and later times, we think
that all known evidence bearing on the point goes to prove that,
"following their inception, they, in common with those of older
- date, were never changed except 1) to be periodically accentu-
ated, 2) to have their axes migrate slightly landward, like the
summit of a wave, in correspondence with effects of active com-
pression and subsequent gravitational adjustments, and 3) to
be modified in their relations to the general plan of crustal
folding by the development of folds of subsequent origin.

We agree with Walcott’s conclusion that in Lower Cambrie
time the greater part of the interior of the continent was land,
and that the first Paleozoic subsidence of the interior and the
real birth of the Mississippian sea occurred with what we term
the St Croix invasion.

a Rhythmic pulsations. There is a rhythmic relation between
_ the successive grand subsidences and emergences of the interior
_ of the continent that we believe should be the basis of a revised
€lassification of the rocks of North America. Such relation was
indicated by Amos Eaton and later by Newberry and others.
_ Each system should begin with a subsidence and end with an
_ emergence. While such a classification will be in some respects
_ different from the one now in use, and its adoption therefore

-

ond b 4 “au wa 1} rok al ¢. i |
: ya] ae 28 Ree ra RE wit 7 1

i
ice

" Beckmantown, we fail: tos ythi ; even appt
sea conditions in any othe s -diment Babs oi
On the contrary, there is PAW Aes a tl
Paleozoic time the “shift of relative ieveley
land was never great outside of the area of ‘the b
scribed. Sometimes the sea was so shallow as t fi
flats, in other cases the Jand was so near sea level th ha it er
was practically nil, but in other cases again, the lan¢ was :
enough to be subject to erosive agencies, the effects of - be
are now more or less obviously preserved in unconform
stratification. These unconformities however, are in b
cases so clear that the stratigraphic discordance may t
nized in any given exposure, but their recognition depe: ;
most cases on the absence in a section of a zone or for
observed in other sections. Sometimes, as on the west fla: re
Cincinnati axis in middle Tennessee, where Upper Deve | ic td
even Lower Carbonic may rest on Middle Trenton, the evidence —
of unconformity is so slight that without fossils it would —
scarcely be detected. re

-
os 4

Principal submergences and emergences. The first Re
Paleozoic submergence in North America resulted in what we
have called the St Croix invasion. It embraced nearly all of that
part of the Algonkian continent lying between the Rocky moun-
tain protaxis and the Appalachian protaxis south of the Cana-
dian shield. This subsidence gave birth to the Mississippian
sea, and the movement accentuated a Precambrice fold under
the Lower Cambrie sea extending from Alabama to Gaspé. The
northern part of this fold we call the Green mountain barrier,
while its southern half is termed the Chilhowee barrier.

The submergence inaugurated by the St Croix invasion cul-
minated in Beekmantown or “ Calciferous” time, when more
of the continent was under water and the sea probably pee
than at any subsequent period.

rier and the southern end as the Rome barrier. There is
ns me reason to believe that the Cincinnati axis or parma had its
Jj inception in this second movement, though it did not reach the
‘surface of the sea till long after, i. e., about the close of the’
‘Black fiver, ut GOR
iat The third pronounced movement occurred at the close of the
3 - Ordovicic, when the elevation begun at the close of the Frank-
fort culminated in the emergence of apparently the whole con-
- tinent, It gave birth to the Taconic mountains and to a third
long Appalachian fold, called the Helderbergian fold or barrier,
_ that excluded the waters of the Mississippian sea from the
E Cumberland basin, which thereafter was occupied by Atlantic
| | waters till the close of the Esopus.
a _ The next i invasion of the Mississippian sea began possibly very
goon after the Richmond emergence, bringing in the Medina,
_ Clinton, Niagara and Guelph faunas, the sea apparently spread-
_ ing a little farther with each succeeding formation. Then a
E- period of emergence set in, continuing in the Mississippian proy-
- ince till Onondaga time, if we disregard the geographically
- limited Helderbergian invasion of Tennessee and southern
Illinois. :
+The period of submergence following this gradual emergence
_ of the Mississippian province also was one of slow action, begin-
_ ning with very late Oriskany or Esopus time and continuing
apparently into the Lower Carbonic. However, considerable
land areas were developed toward the close of the Devonie, so
_ that the rocks of this system also bear evidence of, first a peri-
4 odically progressing submergence and then an emergence like
_- those more clearly shown for the preceding systems. Similar
movements are indicated again for the Lower Carbonic and the
Upper Carbonic. 2

ing the chat and St :

uniformly represented there by. the L

of the Stones river, | the last iv

The second invasion was very difterent { of t
river. It came in from both the peR oy pe Bie: :
that from the former source advancing rapidly a ne a la
the coarse deposits of the Oriskany, that from be
tion progressing apparently more slowly and — lying

the limestones of Onondaga age; and, meeting, their’
faunas commingled in the Decewvyille formation describe

Effectiveness of folds as barriers to seas. The Green mou
Chilhowee barrier, the first and oldest fold west of t -\pp
lachian protaxis, was not crossed by the sea from the al lose « f
the Beekmantown age to early Silurie time, but throu ug
whole of Siluric and some of Devonic time it was ineff e
as a barrier to the Atlantic, which passed over it probably it 2
the region of Maryland. These same waters also crossed |
Appalachian valley barrier, but a younger fold (Helderbergia
barrier), lying to the west of the other two, still prevented t
Atlantic from joining the Mississippian sea throughout the nn
from Medina well into the Oriskany. The union of the two seas,
however, was effected during late Oriskany, in Marcellus and ©
possibly again during a portion of Portage time (Genesee). ‘
The Mississippian sea crossed the Appalachian valley barrier a
from southwestern Virginia northward, to east central New —
York, excepting the intervals when the north Atlantie by way 4
of the St Lawrence channel crossed it with the Normans kill —
and Utica deposits and faunas, from Lowville to close of Frank-
fort time. Previous to this time, and immediately succeeding —
the formation of the Appalachian fold, the Atlantic invaded the —
terminal thirds of the Appalachian trough, filling the southern —
Lenoir basin, which was confined between the effective Rome —
and Chilhowee barriers, while it occupied two narrow basins in 4

REPORT OF THE STATE PALEONTOLOGIST 1901 —- 663

- the north, the Levis channel on the east, the Chazy bay on the
west side of the Quebec barrier. Though the Chazy bay ex-
ended some distance up the Ottawa valley, there was no com-
& munication between the Atlantic and Mississippian seas at this
ia time, a great land area to the west of the bay affording effectual
separation.
- Communication between the Atlantic and the Mississippian
Seas occurred at least once besides the Normans kill, Utica, and
Deyonic connections just mentioned. We refer to the communi-
cation that probably began during late Upper Cambric and
either continued through or was revived during Beekmantown
time.

Basis for more exact faunal and phyletic studies. We have pointed
out the Paleozoic periods when the Atlantic and Mississippian
seas were separated from each other and also when they were in
communication. The relations of the Mississippian sea to the
Arctic, northern Pacific and Gulf of Mexico remain in great part
yet to be determined. Reliable data are difficult to secure, yet
they are not so few as to discourage the hope of ultimate suc-
cess. When the more essential facts are known, paleontologists
will learn to discriminate between the foreign and indigenous
elements of our fossil faunas, and incidentally these new facts
will throw much light on general geology and organic evolution.
They will not then be so likely to arrange heterogenous specific
elements as members of one line of descent, nor will they be
so eager to identify or throw together species and genera that
better and fuller information may prove to represent even dif-

;
‘
é -
q
4

ferent lines of development. The species and genera may have
much in common, but the investigator will pause and look care-
fully into their derivation, both biologic and geographic, before
he will feel justified in pronouncing them identical. In short,
we shall secure more critical, and therefore more reliable results,
and these will bear sound fruit, not only in the domain of pure
biology, but also in stratigraphic geology. The farther we pro-
gress along the lines indicated, the more exact will our corre-
lations become. Indeed, even extra-continental correlations are
not beyond approximate exactitude.

state paleontologist. ‘The existence of a
channel parallel to the orograph ¢ fe
border is recognized by the writer es
the proper apprehension of the sequence «ane g
tions of the New York faunas. The full value of th q
tions set forth by the accomplished authors i e |
measured when time has permitted an adjustment of co
ing evidence by a more complete array of facts. be ;
ing, however, it is in part intended to show, irres,
finer analysis of the shore topography, in wiiats }
Devonie faunas of New York indicate the influer a of 8
Appalachian channel. ee tc

By an indigene fauna is meant, in this paper, one which, ti kK
ing possession of the marine province at an early date, h ei he |
ground (subject to variations in its species combination) for
long period, during which may have occurred yarious m inor ir
vasions. This is the correct significance of the term, as i |
indigene fauna is alien in its inception. “i

The Appalachian gulf, or marine water of the New York —
Devonic, had its northern coast line at the opening of this
period probably not far south of the present south line of
Lake Ontario and the course of the Mohawk river. This state-
ment is made assumptively, as the northern shoreward edges
of the sediments of the period have been removed. We may
Say with some assurance that this continent line was
no farther south; it may however have been situated

— down: the Appalachians through Pennsylvania, Maryland and
3 Virginia. Outside and eastward of the gulf, separated theze-
i from by a narrow land bar, was, we may confidently believe,
4 ~ in accordance with Messrs Ulrich and Schuchert’s deductions, a
stretch of water probably of no great width as far as Albany,
-Tkewise extending parallel with the Appalachian trend. From
the evidences of early Devonic rocks in Massachusetts, New
Brainpshire and Maine we have reason to believe this area
widened irregularly to the Atlantic and passed far beyond
the head of the gulf to the northward. Southward down
this waterway traveled the congeries of species which in the
early Devonic entered New York from a center of prolific de-
velopment and departure in Gaspé and New Brunswick, and in
Siluric times from regions of the east still more remote. This
is a condition which had existed long before the Devonic, and
the same waters had served as a passage for the migration of
Species into eastern New York. While the early Devonic saw
the continuance of the condition, the later stages of the time
- witnessed its disruption and discontinuance.

- The earliest of the Devonic faunas of New York is that of the
Helderbergian. Geographically the Helderberg sediments, as
shown by Ulrich and Schuchert, were laid down east of the land
barrier and on the west shore of the Appalachian strait and

Q

{ Helderbergian fauna

:

¢

F

4

in our view, also along the widening northern opening of this

rest through Ontario and Manitoba, the southern extende ee ae ‘

mvaltipiied to ite climax Whe: os erbe
thus an invader from the northeas tom Bs
separated its first assession from the Aa vada an
a state of degradation So extensive that, at tl threes
of its presence, transgression over this barrier > fa
effected, but not a transgression which extended far,
barrier remained an obstacle to free migration.
The Helderbergian, however, did not gain poss m ¢
extensive area in New York during its earliest. mani f i .
its species commingled in some measure with the frail
congeries on the ground of central and western New
which had endeavored to reinstate itself with the gradual sie
ening of the Salina sea, but in later stages of its existence t he
reintegration of the barrier shut out from the area of the App
achian gulf all evidence of its final phases (Becraft, Kings
(—Port Ewen) beds). The area of the Helderberg in New York
was its fruitful center of dispersion, and thence its travels were- %
southward along the barrier, probably around its southern :;
termination, and from there into the Appalachian gulf in the
region of western Tennessee, Illinois and Indian Territory. ’

+2 7

.
io.
™

Oriskany fauna

From the same direction and along the same thoroughfare a
came the Oriskany, its center of variation and dispersion un-
questionably being in the region of Gaspé bay, where now its
species are dispersed through 800 feet of limestone. Leaving
behind it species which may have survived in the Gas 96
sandstones to a later period of Devonic time, it followed in the
train of the Helderberg fauna, manifesting itself most perfeetly
in the silicious limestones of Columbia and Ulster counties,

i s

en i ee . ie on
ees Fr aye a Sig
; =~ \&
l a} »- » ‘

REPORT OF THE STATE PALEONTOLOGIST 1901 667.

e ( Naturally its fauna includes some Helderbergian species, partly

| picked up in its travels hither from Gaspé and partly found on
the ground on its arrival in New York. As pointed out in our
previous studies of this fauna, its species trangressed for a very
brief period the eastern limits of calcareous deposit and spread
themselves westward over the irregular, deeply embayed and
probably rocky coast line of central New York and Ontario.

Onondaga fauna

Primarily this fauna is of reef-building corals, and entered
the state from the west, where its reefs and attendant organ-
isms attained their greatest prolixity. The lessening and dis-
appearance of the coral facies eastward and the final loss of the
limestone deposit evince this derivation. Any submarine bar-
rier in the east however was so deeply submerged at this epoch
as not to interfere with the deposition of chert-bearing lime-
stone in Columbia county east of the Hudson river. The east
presents in the arenaceous beds of the Cauda-galli and Scho-
harie grit a facies which is not elsewhere seen. In clastic
character, there is excellent reason for associating these beds
directly with the deposition of Oriskany sediments as
a closing stage thereof, and indeed several elements of
the striking Schoharie fauna indicate derived relations to the
Oriskany. This might be predicated of the trilobites specially,
of the brachiopods and lamellibranchs in part, but not of the
most conspicuous element of the fauna, the cephalopods. For
the origin of the latter we have yet to search; they may have
entered New York from the west with the fauna of the lime-
stone and have wandered into the shallow waters where Scho-
harie sediment was depositing; they may have, on the other —
hand, come in from some source, northeast or southeast, as yet
unknown to us, and hence be related ancestrally to similar forms
of the overlying Onondaga limestone. Present evidence seems
to favor the former conclusion without disparagement to the
genetic relations of these cephalopods to those of the Onondaga.
It seems justifiable however to assert that the fauna of the
Onondaga period as a whole, with its noteworthy coral, trilo-

to ‘tlie oind-of ‘the barrier wail Gaeubs Salk EE
The latter seems specially probable of the

2 | | . = e ~y
As the Onondaga limestone fauna came in from. I mck

——

it withdrew westward. In the latest stages of its i grat ti
it brought in the cephalopod Agoniatites me
but when this species had penetrated to eastern nuieal
ground had been occupied for some time by shallowed and f
waters, wherein were depositing the black muds of the i
lus shale with its accompanying singular fauna. Early } far
cellus deposits in eastern New York were thus contemporane- _
ous with late Onondaga deposits in western New York. This ;
being true, the Marcellus fauna entered the New York area of ee
the gulf from the southeast or from the direction of the eastern a |
shore. The effect of the putative eastern barrier and its accom- “a
panying northeast channel is now no longer perceptible saye as
we ascribe to the submergence of the latter in part the befoul-

ing of the waters.
Fauna of the Agoniatites limestone

It has just been stated that Agoniatites expansus
came into New York from the west in the closing stage of )
Onondaga time. The limestone to which it appertains forms
a very distinct band in the Marcellus section of eastern and
central New York, and associated with it is a small and exelu-
sive congeries of species, with some which belong to the fauna
of the shales. So far as concerns the peculiar species which
characterize the fauna, they have probably all been derived
from the same direction at the same time as Agon. ex-
pansus.

¢ of the fauna, for a calcareous layer just at the base of the Mar-

cies commingled with others surviving from the Onondaga fauna,
but the Stafford affords a pure Hamilton fauna. The incursion
S of this congeries in this manner is very significant; the lime-
. _ stone and its contents are lost east of Ontario county, but from
there to the western limit of the state its course is unbroken.
Thus it clearly indicates that the Hamilton fauna, both in this
; prenuncial expression and in its normal return, after its retreat
had been covered by a considerable period of deposition in the

west; whether from the northwest, through the opening of the
shore line up through Manitoba and thence westward through

ne Ee ee a ee
~~ , : ~ ’ re, mt
’ pm 4 4 7 .
* .

ing the Devonic shore line of eastern South America, where it
arrived by shore from Africa and its center of dispersion in

Belgium and the Eifel or, again, along the assumed north

‘ Atlantic land line, can not yet be determined.

2 Tully fauna
This fauna is essentially constituted of derivatives from the
Hamilton with the addition of two brachiopods of world-wide
distribution, Hypothyris cuboides and Schizo-
phoria tulliensis (cf. 8S. striatula Schloth.). The
former is an excellent index fossil of the lowest Upper Devonie,
the latter a belated newcomer of Middle Devonic habit. So far
as the special expression of the fauna imparted by these two
Species is concerned, it does not elsewhere manifest itself in

, “caieage limestone goes no farther west as a inca : a 2
‘Goat same i ae Stafford limestone contains = oy

Eatin Rees. This is not actually the earliest pee “

3 _cellus shales in western New York also carries Hamilton spe- _

gradually clearing Marcellus waters, entered the state from the

3 Siberia to the Ural Devonic sea, or up from the south, skirt-

tae

a ‘ ~—6dTCTLIS a ae wes
.\ ~< a sick sang be “
4 ye 4 . : onl a
ez the bla ¢ -
-

New oe , n
Portage oe ma is |
the northwest... It has. ‘ieee nught ir
Hamilton fauna which preceded it. on the groune
geries of oceanic organisms which Loeede ss ronstitute
of Manticoceras intumescens, Bh pe ked
parts of the world but nowhere with a more aa :
here. Eastward of Cayuga lake its integrity is lost by me
with the contemporaneous Ithaca fauna. The mig: at
of this pelagic fauna has been traced toward iia ort
through Manitoba into Siberia, thence — through BR issiz
Westphalia. Where it was originally autochthonal is 1 ot cer-
tain; perhaps Westphalia was its home, but in New Yo where
its fauna became extensive, it was alien and short-lived. — ee zc,

Ithaca fauna vi ae a

Contemporaneously with the Naples fauna in western } e) v +4
York the Ithaca fauna held the field in central New York ap-— 7
proximately, except in its latest stages, from Cayuga lake bs sh
the west to the Chenango valley on the east.

The Ithaca fauna is genetically sequential to the fauna aru
the Hamilton epoch. Its species are at first identical with
those; then variations superinduced on these specific types man-
ifest themselves, and in the event the fauna in its totality is
clearly distinct from its ancestor. Hemmed in on the east
by the barrier which made the Oneonta waters a lagoon, and —
on the west by the invading Naples fauna, it found fayorable
opportunity for multiplication and variation on ancestral

a
ee.

a

‘The authors of the preceding paper regard the Naples invasion as from
the Atlantic. This is an assumption unsupported by any eyidence known
to the writer,

REPORT OF THE STATE PALEONTOLOGIST 1901 - 671

ground. It is indigene, for its ancestry had taken and lost pos-
‘sessions early in Marcellus time by invasions from the west, re-
taken and held possession from the beginning of Hamilton
time. It is to be noted that through a part of the extent of the
Ithaca sediments there is nothing separating them from the
Hamilton beds below, the Tully limestone and Genesee shale.
feathering west of the Chenango valley.

Oveonta fauna

Contemporaneous with the latter part of Ithaca sedi-
mentation was the sparse fauna of the Oneonta sandstones.
These we believe to have been deposited in a narrow coastal
lagoon, and its few characteristic organisms, Amnigenia
* catskillensis, Estheria membranacea,. are of
fresh-water habit. The latter occurs in the Old Red lakes
of northern Scotland, species of the former in nonmarine de-
posits of Ireland and the Eifel. We are left to surmise that
these species found their way into New York by fresh or —
brackish water passage from the Old Red lakes of Nova Scotia
(Arisaig) and Quebec (Gaspé).

The Catskill. The Catskill represents a continuation of One-
onta sedimentation; that is, deposition in a deep embayment but
with freer access to the open waters of the gulf, thus constitut-
ing a long and narrow estuary extending far southward parallel
to Appalachian trend. It may well be compared to the condi-
tions now existing in the Lake of Stennis in the Orkney main-
land as described by Hugh Miller, in which the upper reaches
are fresh and bear a fresh or depauperated brackish water
fauna while the lower parts are salt and marine. We know
that this condition (including the deposits of the Oneonta) pre-
vailed in eastern New York from the close of the Hamilton
through Portage and Chemung time and in southern New York
continued into the early Carbonie.

- Chemung fauna
The main body of the Chemung fauna is the direct derivative
along the long line of descent from the Hamilton through the

— =

tus ark ths Eins octeee ‘deinen eve Ly
expression of the single New York fauna of Devoni
may be properly characterized as indigene.

;

FiaG. *

1 Greater portion of a large frond party»
matrix. The segments are somewhat macer
show the effect of current dragging. N: vat

Chemung, at East Windsor N. Y. New Yor

museum.

CHEMUNG ALGA

Rep N.Y. State Paleontologist 1901

Plate 3

GS Barkentin.del

Phil. Ast, lith.

><
4
“4

te
¢
:
Z

wiG.. -y
1 Portions of several segments, probably be
same frond or the same tuft. The diferent p

r at different levels in the bed, the le

; out at the back side of the slab. ‘Nat iral size.
_ Same slab as pl. 3. | on Be
<a 2 Isolated portions of two segments showin more a

tinetly the mode of division, the aspect of the t
2 portions and the lamina. Natural size. a ze
Catskill at Factoryville, Wyoming co. Pa. No. 2

Lacoe collection, United States national muse nies a.
- an - . "

a

4

ee ee on es

‘Jap unueyIEg S95

uM IsVv “Wd

yaeld ost 1s1Sorewoeted 11S AN dou

VOTV DNOWAHO

. ot ee é :
Eunoa accola Clarke — —
- ‘oy MEE
ete. | (See pl. 6) ae
FIG. ee

“a at .

-
¥

ne gens Py + *

el

Beekmantown graptolite shales.
mo:

Ae dN pt ee eee
4 a
_
>
——
be)
3
0Q
(a*)
oe
3
bo)
3
S
p)
—
<j
95
—
=<
ie)
——
:
5
gm |
—
feel
ct
o
=)
ct
co
ag
ee)
2
8

, aS. Barkentin.de JLB Ly n Co, State Printer Phil. Ast, lith.

Se Sh . Sil ae
= 2
ee or
* By
n “
: =
‘
”
~
.
7
a
fe
a ~
——
=_ -

te

ery
Boh. Cis Pe

7

brachial valve is here again not a ns
2 A pedicle valve with the margins of the pedicle slit appr
mately entire for most of their extent, though | hes
apart.
Beekmantown Sreptolite shales. Deep a
co. NL. Xs

tor

1

Ast, |

al.

Ph

nter

tate Pri

iS)

’

Lyon Co.

J

G.S.Barkentin. del.

}
$y

“> “ea

eat SS ahs .;
ae 1 The half of an infolded pedicle Saniaiaatas @

Seah ing extending for the full radius of the shell,
of the infolded portion of the valve is visible Be
phery of the shield.

Portage beds. Tannery gully, Naples N. Ys at an he
just above the final appearance of the Naples fauna,

Phil. Ast, lith.

nter

7
A

=
ay
Me

. Lyon Co, Sta

B

G.S.Barkentin.del.

‘ at >

+ 1 sd ¥ 7 .

e @ Ps) + ee

~/ «4 7 a ‘ J
Be Se ble ee Pee
ate i a ae)
Orbiculoidea ? magn

: ee; road ip >
. " ”

be " a a? 7
a a, i
+ < :
a >

= Fe

FIG. eae ey
1 A large depressed conical shield believed to
brachial valve of this organism. Drawn ‘ron
cast. ™
Ithaca beds. Truxton N. Y.

G.S.Barkentin.del.

ORBICULOIDEA.

Rep Paleontologist 1901. Plate 8

. Phil. Ast, lith.
GS Barkentin del J.B. Lyon Co, State Printer eS

INDEX

Page numbers referring to descriptions of fossils are printed in black

face type.

The superior figures tell the exact place on the page in ninths;

e. ¢g.623° means page 6238, beginning in the third ninthof the page, i. e.

about one third of the way down.

Actinopteria, 655°.

Additions to paleontologic collec-
tions, 461°-68°.

Adirondacks, maximum of com-
pression east of, 648°.

Aeglina, 640*, 641°.

Agelacrinites buttsi, 527°, 528°.

Agnostus, 640*, 641’.

Agoniatites expansus, 668*, 668".

Agoniatites limestone, 436°; fauna,
668".

Albion quadrangle, contact lines of
Upper Siluric, 519*-21°,

Ambocoelia umbonata, 623*, 624+.

var. gregaria, 622%,

American association for the ad-
vancement of science, memorial
tablet for the Emmons house,
4527-56.

American paleozoic fossils, record
of localities, 468°-516.

Ami, cited, 558°, 559°, 567°, 5767, 576%,
579", 643°.

Amnigenia catskillensis, 671%.

Ampyx, 640*, 6417.

Annelids, 544°.

Appalachian geology, 633'-63°.

Appalachian Mediterranean, 649*.

Appalachian valley barrier, 638°,
6617.

Appalachian valley trough, 688’.

Arey, Albert L., cited, 4827.

Arthracantha depressa, 624°.

Association of American geologists,
organization, 452°.

Athens trough, 644°.

Athyris angelica, 526°, 527°.

eora. 526°, 527°,
polita, 527’.

Atrypa, 623°,
aspera, 628°.
hystrix, 624°.
reticularis, 622%,

Aviculopecten, 526°.

Axonophora, 571’,

Bactrites, 655°.
Barrois, cited, 5637.
Bays sandstone, 645°,
Beekmantown dolomite, exposures,.
534°, 536%, 5387’, 537%.
Beekmantown formation, 6377;
study of fauna, 427*; in Rensse-
laer county, graptolite (Levis)
facies, by Rudolf Ruedemann,
D46-75.
Beekmantown time, 660°.
Bell, Robert, mentioned, 434°.
Bellerophon maera, 526°.
Beloceras, 656°.
Bertrand, cited, 649°.
Billings, E., referred to, 633°.
Black river invasion, 641°.
Bothriolepis, 528°, 528°.
Brachiopods, 430°, 527°,
544°, 554%, 5568, 566+.
Brockport quadrangle, contact lines
of upper Siluric formations, 517'-
23.
Brogger, cited, 563%.
Bronn, cited, 599*.
Bryograptus, 550°, 555°, 584°, 586°,
588°, 589°.
sp. nov. 554*, 555°, 5561.
kjerulfi, 5567.
Buthotrephis gracilis, 597°.
subnodosa, 597°.
Butts, Charles, referred to,
442°; paleontologic work,
524%,

533*, 539°,

441°,
4469,

« a Siluric, line of division,

(580
Campbet, M. R., referred to, 441’,

Meet a lake region, paleon-
tologic and stratigraphic map,

422°-24°,
Carbonic strata, 6567-58.

Carbonic and Devonic, line of di-

vision, 524°.
Cardiocaris, 606-15, 610°,
Carruthers, cited, 601°.
Caryoearis, sp. 554°.
curvilatus, 556°.
cf. oblongus, 556".
Cashaqua shale, 617°,

Catalogue of type specimens, 444°-

46°; of fossil faunas, 446°.
Catskill formation, 524’, 671°.
Cattaraugus beds, 525°.
Cayugan emergence, 648".
Cephalopods, 430°.
Ceratodictya annulata, 624’.
Chazy basin, 638°, 639+.
Chazy limestone, 639°;
fauna, 427*
Chemung beds, traverses of, 524°.
Chemung group, fossil alga, 593-605;
fauna, 671°-72°,
Chickamaugua limestone, 645°.
Chilhowee barrier, 638°.
Chiropteris reichii, 599*.
Chonetes, 623‘, 628°,
scitula, 526°, 5277
Chonostrophia complanata, 653°,
Christiania, 6412.
Cimitaria corrugata, 624°.
Cladochonous, 628?, 628°,
Clarke, John M., field work, 425°:
report on contact lines of upper

study of

Clinton beds, limestone 1
428°-31°; exposures, 517%, {
Clonograptus, 561°, -
586°", 588°.
flexilis, 582', 582°.
rigidus, 5821, 585.
Coenograptus, 581°, 5847, > 3 ee
gen. nov, et sp, nov. 566%
gracilis, 583°, : os .

Conocephalites verrucosus, 534", ’
534°, 540°, 545°, x:
Corralline limestone, 650°. =p hel

Corals, memoir on, 442°,
Crenipecten, 526°.
Cryptograptus, 569°, 571°, 573°.
antennarius, 439°, 570%, arr,
572, 574°. a Fe
Ctenodus, 528°, 528°. t
Ctenograptus, 581°.
Cuba sandstone, 525°.
Cumberland basin, 638’,
649*, 653°.
Cushing, cited, 538°, 542*,
Cyrtoclymenia, 656°.

645", 647°

Dale, T. Nelson, investigations car
ried on by, 550°; cited, 643°.

Dalmanites limulurus, 517°

Dames, cited, 611°.

Dana, cited, 646°, 651°, 4

Darton, cited, 654°.

ptus, 4397, 5715.
eancellatum, 570°,

nic, in eastern North America,
et we casi and = alien

‘Dicellograptus, 608’, 640°.
_ Dichograptus, 487°, 438%, 550°, 556°,
bes 561", 562°, 5837, 584°, 586°.
som age. 57 .1*.
_ flexilis, 559°.
logani, 559".
octobrachiatus, 554°,
570 74-580", 583°.
Dicranograptus, 608".
Dictyonema, 489°, 571°.
-§p. nov. 555", 570°, 570’.
cancellatum, 570°.
cf. delicatulum, 565°
flabelliforme, 5508, 551°, 559°.
Dictyophyton tuberosum, 626+.
Dictyopteris delicatula, 604’.
Dictyospongia, 526°, 528°.
Didymograptus, 556°, 557°, 569°, 568*,

556°, 565°,

581%, 584*, 586°, 586°, 588°.
Sp. nov. 556°, 570%.
bifidus, 488°, 4388", 563’, 564°,

565", 566°, 566°, 567, 567°, 567°,
568°, 568°, 568°, 5697, 5697, 569°,
Me. So, olo, ola, O14, 014°,
576°, 592°.

cf. bifidus, 569*.

constrictus, 562°.

extensus, 556°, 568°.

filiformis, 556°.

gibberulus, 588’.

var. nanus, 5708.

| Diplograptidae, 571°.

es 4387, 36r, 67, se
if. similis, 566%." +* 3 iS bs

Diplograptus, 571’, 573°, .e
Sp: nes. STL BPR A jee
dentatus, 570*, 570°, 570°, 571%, a

572°, 573%, 5742, 5747, oe Fr
inutilis, 489*, 570°. i aa
pristiniformis, 489", 570°.

Dipterocaris, 612°, 612°, 613", 613°.

Discinocaris, 606-15, 609°, 610°.
browniana, 609%, 610°.
gigantea, 608°, 609°, 609°. ae

Eaton, Amos, cited, 659°.
Eatonia peculiaris, 653%.
Edmondia, 526°, 527°.
Eichwald, cited, 604*.
Biles, G. L., cited, 560*,
569", 573°, 573%, 582°.
Ells, R. W., cited, 529%, 558°.
Emmons, Ebenezer, cited, 427, B2OF
Emmons, Ebenezer, jr, statement
dictated to John M. Clarke by,
455°-56".
Emmons house,
for, 4527-56".
Estheria membranacea, 671*.
Etheridge, jr, cited, 564°.

561°, 568°,

memorial tablet

~ Euomphatlus hecale, 526°.

Eunoa, a new genus of paleozoic

. brachiopods by J. M. Clarke,
606-15.
Eunoa accola, 571°, 607'-10°; ex-

planation of plates, 678, 680.
Eurypterus, 421°, 422°.
Ewing, Charles, paleontologie work,
429°: referred to, 442°.
Explanation of plates, 673-84.

Favosites, 518*.
Field staff, personnel, 442°.
Fontainea, 599°.

-Gardeau shale and flagstones, 617°*-

18°.

Gastropods, 434’,
539°, 544°, 554°.
Geinitz, cited, 604*.
Geologic map of the state, contribu-

tions to, 448°,

Gephyroceras, 656.

Gilbert, G. K., mentioned, 428°.

Glenn, L. C., referred to, 441", 442°;

paleontologic work, 524°.

Glossograptus, 571°, 573°,

sp. nov. 571°. ~

Goniatite limestone, 436%.

Goniatites, 628°.

Goniograptus, 561°, 568%, 576°, 580",
581°, 583*, 583°, 585', 587°, 591°,
591°, 592°.

sp. nov. 556°, 566".
thureaui, 439°, 5567,
. 566°, 576-92.

var. postremus, 580°.

Géppert, cited, 598°, 600*, 603%, 604°.

Grabau, A. W., paleontologic work,

435°, 526°, 533%, -

564", 557%,

429°; mentioned, 431', 442°; cited,
451’, 652°,
Grammysia elliptica, 624°,
Graptolite (Levis) facies of the

Beekmantown formation in Rens-
selaer county, by Rudolf Ruede-
mann, 546-75.
Graptolite fauna, 437°,
Graptolite schists, 562°,
Graptolithus milesi, 582°,
richardsoni, 563°.

"Fue, “Myron Te sen to, 4a, :

-Hall, T. S., cited, 569°.

contortuplicatus, ¢ 64
dechenianus, 598",
6017, 602", 602%, 60
603°, 604°, hs.
distans, 604*.
gracilis, 604°,
lineatus, 604°. i
lusaticus, 604,
reichii, 599°, 5997. ee
Hall, E. B., acknowledgm« nen
451°; gift to museum, 594.
Hall, James, cited, 432’, ase,
439°, 557°, 572%, 582", 654°; sale of
fossils, 445°; statement dictated | &
John M. Clarke by, 455%; men-—
tioned, 606*, 616°, 617°, 618*, 618°. vie

E ty

et
An

Hamilton fauna, 669". thd
Hartnagel, C. A., collections ae
by, 420°; referred to, 442"; com- |

pilation of catalogue of fossil ‘-
faunas, 446°; paleontologic work, —
446°. Ses
Helderberg basin, 647%. re
Helderbergian barrier, 661°.
Helderbergian fauna, 665%-66".
Helderbergian invasion, 648°-51°,
Holm, cited, 563°, 581°,. 583°, 5844,
591°. Ge
Hologr ptus, 581°, 583°, 584° “a
Holoptychius, 528*. .
americanus, 528°.
Holzapfel, cited, 611*, 611°.
Hopkinson, cited, 562°.
Hostinella hostinensis, 602°,

<i
=
r;

LE

ology, 448°-49°.

a: Sibberalas, 5887.
> - par. napus, 570°.

i Ithaca fauna, 419°-215, 446°-47', 670°-
ax 7. 3

Jackson, R. T., cited, 587%, 587°.

_ Jones, T. R., cited, 608°, 609°.

Kayser, cited, 610°.

Kemp, J. F., cited, 540°.
Kidston, cited, 602°.
Kjerulf, cited, 563‘.

Knoxville trough, 644°.

Kiimmel, cited, 641°.

Lapworth, cited, 553°, 557°, 558’,
Ga aGe, 567, 568, 572°, 573°,
608°, 608’.

Lenoir basin, 638°, 644’, 645°.
Leperditia, 649°.
Lepidodendron
602%.
nothum, 602’.

gaspianum, 602’,

- Leptodesma, 623°.

eurvatum, 528".
longispinum, 527°.

maclurii, 5287.

matheri, 527°.

mortoni, 526°, 527°.
mytiliforme, 528°.

orodes, 527°, 528".

potens, 526°, 527°.

var. juvenis, 526°, 527°.

_ Lesquereux, cited, 598".

» state publications on

Leptostrophia mucronata, oe, :

Levis beds, 558°.
Levis channel, 638", 639+.
Levis facies of the Beekmantown —

formation in Rensselaer coun %

546-75.
Lichenalia, 429°,

Limestones of Beez Cambric age,

637°.
Lingula, 606°.
quebecensis,
571°, 606°.

438°, 566%, 571,

Lingulella, 533°, 533°, 534°, 5342, 534’,

536°, 540°, 541*, 545*.
acuminata, 540°, 544°, 545°, 545°.
Lingulepis minima, 540°, 545°.
Linnarsson, cited, 562°.
Liorhynchus, 623%, 655°.
mesacostalis, 624°.
quadricostatus, 622°.

-Loealities of American paleozoic

fossils, record of, 468°-516.

Locality record of museum speci-
mens, 456°.

Lockport dolomites, exposures, 517*-
18°, 520*-21?.

Logan, Sir
434°, 435°,
651°.

Loganograptus, 487%, 5845.

logani, 556’, 564*, 570°, 571°, 583,
583%.

Loomis, F. B., paleontologie studies,
448*.

Lorraine sea, 643%,

Lower Cambric trough, 635°-36°.

Lower Dicellograptus fauna, 6407.

Lunulicardium fragile, 617°

Luther, D. D., fossils collected by,
419°; field investigations, 421°,
424°, 4257, 426'; report on contact
lines of Upper Siluric formations
on Brockport and Medina quad-

William,
633°; cited, 5298,

mentioned,
558°,

7

wh

iF intumescens, 610°, 656", 670".

oxy, 628". ‘ =

--pattersoni, 613°.

Marcellus formation, 435°-36°; fauna,
668°. .

Marcellus invasion, 654?-55°,

Marr, cited, 561°, 573°, 573°.

Matthew, G. F., cited, 559°, 583’,
636, 642°.

Mattimore, H. §., collections made
by, 420°.

Medina quadrangle, contact lines of
upper Siluric formations, 517-23,
5217-22",

Medina sandstone, exposures, 519’-
20°, 522°.

Megalaspis limbata, 569°.

planilimbata, 569°.

Megalomus, 434’, 435‘,

Mesothyra, 612°.

Mississippian sea, birth of, 636°,
659"; depth of, 660".

Modiola praecedens, 527*.

Moffatt series, 608°-10°.

Monograptus, 608".

Monroe mastodon, 439°-41°.

Monroe shales, 654°.

Morgan, R. F., paleontologic work,
42%; referred to, 442°,

Mount Hermon conglomerate, 525°.

Mytilarea, 526°.

chemungensis, 528%,

Naples fauna, 421', 656°,
Nemagraptus sp.
sp. indet. 570°.
Nematophyton dechenianum,
Newberry, cited, 599°, 659°.

670",
566".

602".

statement of
results of ass irvey
28. ‘S78 ar
Oneonta fauna, 6713,
Onondaga fauna, wre,
Onondaga invasion, 652*, 6
Ophileta, 534’, 534°, 540%, | E 542°
compacta, 545%. eae
Orbiculoidea, 607°, 608", |
sp. 622°,
magnifica, 615". a
explanation of wlaadl sa, a
684. is ‘ts > 4
pl. facing p. 614. =° cet
Ordovicie, in eastern North Amer
637°-47°. :
Oriskany formation, 651°-52°;
666°-67?.
Oriskany invasion, 662%, oe
Orthis, 628", 628°,
tioga, 526°.
Orthoceratites, 628°.
Orthothetes chemungensis, 526°.
Ostracoda, 649".
Oswegan invasion, 647%.
Ottawa bay, 642*.

xe ;

Palaeanatina, 528°,
typa, 527°.
Palaeotrochus praecursor, 624". ‘
Paleontology, index to state pub- 4
lications on, 448*-49*,
Paleozoic corals, memoir on, 442°.

2s referred to, 442°.
s 6112, 612%.
wv, cited, 602%, 603", 603",

;

> hi aieeardia. 612°.
1yllograptus, 4378, 549%, =: BG,

_-«#BBT*, 568°, 584+, 588°, 5904, 640°.

~ age sp. 563’, 563°.

«gp. nov. 570°.

~~ angustifolius, 438", 554’,

63°, 566°, 570°, 571°, 5737.
anna, 438°, 565’, 566°, 566°, 567°,
aor.) ool, dot, 568", 569°,
Sis DL. Olio, Sto, Dla» DI#;
i TG
ilicifolius, 554’, 555°, 566°, 567°.
var. 559.
var. grandis, 556°.
typus, 438’, 557*, 564°, 566°, 566°,
5671, 567%, 568°, 5688, 569°,
cf. typus, 569°, 569+.

Phyllograptus schists, 562°.

Piedboeuf, cited, 602'.

Plates, explanation of, 673-84.

Platyceras, 534°, 542°, 545+,

Pleurograptus, 608’.

Portage fauna, 420°.

Portage sandstones, stratigraphic
value, by D. D. Luther, 616-29.

Potonié, cited, 601°, 604".

Potsdam sandstone of the Lake
Champlain basin, by Gilbert van
Ingen,-427°-28?, 529-45.

Prismodictya, 528*.

Productella, 526°, 527

lachrymosa, 624°.
speciosa, 622%.

a7) aaa

om T, W., paleontologic work,

556°,

ee elegans, 5§
Pterygotus, 421°, 4227.
Ptilograptus, 571°, 571°.
plumosus, 570°.
Ptychoparia, 545‘.
minuta, 534°, 534°, 5407, 5458. =
Ptychopterias, 527%, 528%. eas
Publications, 442°-44°, : |

Quebec barrier, 661°.
Quebee group, 557°.

Rensselaer county, N. Y., grapto-
lite (Levis) facies of the Beek-
mantown formation, by Rudolf
Ruedemann, 546-75.

Retiograptus, 5717.

tentaculatus, 4897, 570*, 5714.

Rhinocaris, 612°.

Rhipidomella musculosa, 653°.

Richmond age, 6457-46°.

Ries, cited, 652°, 654°.

Riley, H. A., referred to, 614°.

Ringueberg, E. N. S., mentioned,
428°...
Rochester shale, fossils from

western New York, 446°; expos-
ures, 517°, 5207, 5227.

Rockwood formation, 645°,

Roemer, F., cited, 610%.

Rome barrier, 644°, 6475, 661°.

Rondout formation, 650°; study of
fossil contents, 421°.

Rothpletz, cited, 599°,

Rouvilligraptus, 564', 581°, 584°.

richardsoni, 569°, )

Rudemann, Rudolf, field work, 425°;
other paleontologie work, 457'; re-
port on contact lines of Upper
Silurie formations on Brockport
and Medina quadrangles, 517-23;
Graptolite (Levis) facies of the
Beekmantown formation in Rens-
selaer county N. Y., 546-75; Mode
of growth and development of

" Sapindopsis variabilis, G00".
-Saporta, cited, G01’.
Sargassum dechenianum, 602°.
Sarle, C. J., cited, 431’.

Schimper, cited, 599*, 601°,

Schizambon, 608°.

Schizobolus, 608°,

Schizocrania, 607°, GOS".

Schizograptus, 581°, 584°.

Schizophoria, 527°

impressa, 624°.
tulliensis, 669°.

Schizotreta, 608°.

Schuchert, Charles, cited, 653°.

& Ulrich, E. O., Paleozoic
seas and barriers in eastern North
America, 633'-63°,

Seolithus canadensis, 5347, 545°,

linearis, 533°, 545°.

Shimer, H. W., paleontologie work,
429°; referred to, 442°,

Siebenthal, cited, 653°.

Siluric, in eastern North America,
647°-48°,

Siluric and Cambrie,
sion, 530,

Simpson, George Bancroft,
morial tribute to, 457-60.

Siphonophora, 590°, 591°.

Skiddaw slates, 560°.

Skunnemunk conglomerate, 654°,

Solms-Laubach, cited, 602°, GOD*.

Spathiocaris, 606-15, 610°,

emersoni, 610°.

Sphenopteris condrusorum, 602°.

Spirifer arenosus, 653°, 6537.

disjunctus, 526*, 526°, 624°,

630", 672°.

line of divi-

me-

650%,

|
|
:
:
-
:

sr Vv ay

Sblawibtst

S By ig ea

Strophalosia, 655° r ,
Stropheodonta cayuta, 62
magniventra, 653", ; ne
vascularia, 653°, we i
Styliolina, 655°. te
Stylonurus excelsior, za a

ae

eo
Taconic mountains, ea, Ch a
Taeniocrada, 603°, G04.
_ lesquereuxi, 603°, —
Temnograptus, 581°, 583°.
cf. multiplex, 556.
Tentaculites, 655°.
Tetragraptus, 487, 458‘, 556°, —
57#, 580'" 5S, DSO, 586", |
589", 590‘, 592°.
sp. nov, 554", 556".
alatus, 56S*,

bigsbyi, 554°, 556°, rs
DOG.

bryonoides, 554°, 560°, 562°, 64,
568°.

crucifer, 56S‘,

fruticosus, 554°, 556%, 564°, 566",
567°, 589", 5897,

aff. hicksii, 556*.

pendens, 566%.

quadribrachiatus,
559", 562°, 563’,
568°, 568°,

serra, 554°, 556°, 563", 564°, 566’,
566°, 569°.

taraxacum, 5897, 589",

Tetragraptus zone, 554*-65".

556", 556°,
564, 566°,

esate, 6547.
" 'Tullberg, cited, 562°, 5631, 569%.
Tully limestone, iron pyrite beds,
_ 447'-48°; fauna, 6697-70".
- Tully aeciancle, areal geology,
424°-

Type poeenens, elas: 444°-46°.

"tT

Ulrich, E. 0., & Schuchert, Charles,
Paleozoic seas and barriers in
eastern north America, 633'-63°.

- Utica invasion, 642°.

Ward, cited, ( - =

- Waterlime strata, study of, aa
2s

Weller, cited, 641°, 650".

White, David, Fossil alga from the ae

Chemung group of New York with
remarks on the genus paints
593-605.
White, T. G., cited, 540°,
Whiteaves, cited, 434+.
Whitfieldella nitida, 429°.

Wilson, John D., assistance from,

436°. x
Wiman, cited, 431°, 584"; mentioned,
591°.
Wolf creek conglomerate, 525°.
Wood, Elvira, cited, 436°.
Woodward, H., cited, 608°, 609”,
610°, 610°, 611°.

Zaphrentis, 521".

635°, 636", 659"; referred t0, 64 es

WwW ee ts copies are rae) a price on xb owe : ee a
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pu blications are in paper covers, unless binding is specified.
seum annual reports 1847-date. Al/ in print to 1892, 50c a
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ese reports are made up of the reports of the director, geologist, paleontolo-
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See

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if 2 Birds. 12+380p.141pl. 1844.
solo ie tes.
dps Reptiles and Amphibia. 7-+98p. pt4 rae 15-+-415p. 1842.
bound together.
7.4 Plates to accompany v.3. Reptiles and Amphibia 23pl. Fishes 79pl. 1842.
f "300 copies with hand-colored plates.
yv.5 pt5 Mollusea. 4+271p. 40pl. pt6 Crustacea. T0p.13pl. 1843-44.
: rand.cnlored plates: Tae bana bomcther oe: P
DIVISION 2BoTANY. Torrey,John. Flora of the State of New York; comprising
full descriptions of all the indigenous and naturalized plants hitherto dis-
covered in the state, with remarks on their economical and medical proper-
ties. 2v. il. pl. sq. Q. Albany 1843. Out of print.

‘y.1 Flora of the State of New York. 12-+4484p. 72pl. 1843.
800 copies with hand-colored plates.

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

DIVISION 3 MINERALOGY. Beck, Lewis C. Mineralogy of New York; comprising
_ 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
4 1842. Out of print.

‘y.1ptl Economical Mineralogy. pt2 Descriptive Mineralogy. 24-++-536p. 1842.

__ 8 plates additional to those printed z as part of the text. _

DIVISION 4 GEOLOGY. Mather, W: W.; Emmons, Ebenezer; Vanuxem, Lardner .
& Hall, James. Gealogy of New York. 4v. il. pl. sq. Q. Albany 1842-43.
Out of print.

‘v.1ptl Mather, W: W. First geological District. 37-4-653p. 46pl. 1843.
y.2pt2 Emmons, Ebenezer. Second geological District. 10+437p.17pl. 1842,
v.3 pts Vannxem, Lardner. Third geological District. 306p. 1842.

at Hall, James. Fourth geological District. 22-+-683p. Map and 19pl.

DIVISION 5 AGRICULTURE. Emmons, Ebenezer. Agriculture of New York; com-
prising an account of the elassification, composition and distribution of the
soils and rocks aud the natural waters of the different geological formations,
together with a condensed view of the meteorology and aericultural produc-
tions of the state. 5v. il. pl. sq. Q. Albany 1846-54. Out of print.

ee of the State, their Composition and Distribution. 11+371p. 21pl

\

parma
”

v2 Org +r eemeian maine of, Lower M Middle we on
‘oS. 0 vp sti Held erberg Group and

er te “me 1859. (3,50) |
it i rae vis

hiesbags cae the Upper Helderberg, Hamilte vl

nd

ung Groups. 11+-1-++428p. 99pl. 50 Pepe
Oe ae vB pil Tobe brancbiata 1. Monomyaria of Ee oper Hl ‘g, Hi
ie and Chemung Groups. 18-+268p. 45p). | $2.50. © af ie re oa!
ee — — Lamellibrancbiata 2, Dimyaria res the Upper Held ? Tam
aye) Portage and Chemang Groups. 62-++293p. 5ipl. _ 1885. $2.5

—— pt2 Gasteropoda, Pteropoda and Cephalopoda ofthe e er r Hel lerber
Hamilton, Portage and Chemung fiaena 2v. 1879, vo Pte |
v.2, 120pl. $2.50 for 2 v. yom ar

v.6 Corals and Bryozoa of the Lower and Upper Helge erg and
Groups. 24-+298p. 67pl. 1887. $2.50. my

v.7 Trilobites and other Crustacea of the mega U Dee
ton, Portage, Chemung and Catskill Groups. 64-++-236p.. 6pl.
supplement to v. 5, pt2. Pteropoda, Cephalopoda aud Anne

$2.50.

y.8ptl Introduction to the Study of the Genera of the Paleozoic B
16-+367p. 44 pl. 1892. $2.50. sd

—— pt2 Paleozoic Brachiopoda, 16+394p. 84pl. 1894.

Museum handbooks 1893-date. 714x12%4 cm.
In quantities, lcent for each 16 pages or less. Single copies pe

below.

H5 New York State Museum. r4p.il. 3c.

Outlines history and work of the musenm; with list of staff and se
publications, 1893. nih
H13 Paleontology. 8p. 2¢. ,

Brief outline of State Museum work in paleontology under bestia Defiaition 5!
Relation to biology; Relation to stratigraphy; History of palo in New
York.
H15 Guide to Excursions in the Fossiliferous Rocks i New York.

I20p. 3&8. .

Itineraries of 32 trips covering nearly the entire series of pelea rocks, p

pared specially for the use of teachers and students desiring to acquaiut them
selves more intimately with the classic rocks of this state.

H16 Entomology. 8p. Out of print.
H17 Geology. Jn preparation.

Maps. Merrill, F: J. H. Economic and Geologic Map of the Stately
of New York. 59x67 cm. 1894. Scale 14 miles to 1 inch. Ow of
print.
New edition in preparation.

Printed also with Museum bulletin 15 and the 48th museum report, v. 1, _

Geologic Map of New York. 1g01. Scale 5 milesto rinch. J
atlas form $3; mounted on rollers $5. Lower Hudson sheet 60c.

The lower Hudson sheet, geologically colored, comprises Rockland, Oran

Dutchess, Putnam, Westchester, New York, Richmond, Kings, Queens an

Nassau counties, and parts of Sullivan, Ulster and Suffolk counties; also north-
eastern New Jersey and part of weste rn Connecticut.

SU
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