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No. 42 Vol. 8

Pome
an
Pa

wr

~

April 1901

HUDSON RIVER BEDS NEAR ALBANY

AND THEIR

_ TAXONOMIC EQUIVALENTS

BY
RUDOLF RUEDEMANN Ph.D.

ALBANY
UNIVERSITY OF THE STATH OF NEW YORK

1901

M74m-No-2000 . Price 25 cents

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Tepearapny by
In cooperatiaen wi
N.Y. State Engi
Geology by Ruda

UNIVERSITY OF THE STATE OF NEW YORK
STATE MUSEUM.

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NIAGARA RIVER

BY

M. {yp

OF THE

AMADEUS W. GRABAU

Topography by U.S. Geological Survey
incosperation withthe

nfinner and Surveyor
Gwology by Amadaua W. Gravau

< :
yereey

ce ee eee

is April 1901

HUDSON RIVER BEDS NEAR ALBANY

AND THEIR

TAXONOMIC EQUIVALENTS

BY
RUDOLF RUEDEMANN Ph.D.

ALBANY
UNIVERSITY OF THE STATE OF NEW YORK

1901 eerian Instiges
“asi
(MAY 281901)

tion _M. >>

1877 Orris H. Warren D.D.

1878 Wurreraw Rew LL.D. - _ fs is
1881 Wim H. Warson M.A. M.D. - -1
1881 Henry E. Turner - = - am eu
1883 Sr Oram MoKmzwar MA. LECD. LLD. DOL. |
1885 Danie, Beach Ph.D. LL.D. - - -
1888 Carrott E. Smira LL.D. - ~ .: Seg
1890 Puy T. Sexton LL.D. - - oe ae

1890 T. Guirrorp Smrra M.A. C.E. LL.D. -
1893 Lewis A. Stmson B.A. LL.D. M.D. = -
1895 Atsert VanpeR VeErR Ph.D. M.D. -
1895 Cuartes R. Skinner M.A. LL.D.
Superintendent of Public Instruction, ex o:
1897 Coustrr 8. Lorp M.A. LL.D. - - = Brookiga
1897 Timorny L. Wooprurr M.A. Lieutenant-Governor, ex pe.
1899 Jonun T. MoDonovuean LL.B. LL.D. is
Secretary of State, ex officio

1900 THomas A. Henprick M.A. LL.D. -—- — Rochester

1901 Bensamin B. Opett sr Governor, ex officio

1901 Ropert C. Pruvn M.A. - - - £— Albany
SECRETARY

Elected by regents . a
1900 James Russert Parsons yr M.A. a

DIRECTORS OF DEPARTMENTS
1888 Mervit Dewey M.A. State library and Home education
1890 James Russert Parsons jr M.A.
Administrative, College and High school dep’ ts
1890 Freperick J. H. Merritt Ph.D. State museum

i i i 519

.
Seta a feeet sake syn cichte oil a(ainlicha gine sin ales = ahd © of <n 5383

Mert a ter Seton pe olilh es.) ttccige cots a.ge'acoe eae « whales « Ra
(Lower Dicellograptus beds) 550 | mee

Epueinaity of faunistic succession in Trenton and Utica beds...... 561
iscussion - the validity of the term, “Hudson river group”....... 564
ae of new ere found in the described shales............ 569
Description CE DPSS Res 2 AE Be IE GORE ear me > RIPng: =f!
MER PEDO OR SP SE Pee ev anee teas ecces OGL
MMIEMCOHC MICO PALES. . eieac-isin+ gacte erin eo tee desiace wees sees eee e088
WOM al ie a ae cn aie vale a aes niele syn * cles oe he canaearieisaccessesesccss OOO

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d bearing shales of Novis kill above the Utica shale ie in
- the Hudson. river beds, asserting their homotaxy with the Lor-
raine beds, Whitfield and Walcott have considered them a part of
the Utica shale formation. Lapworth and Gurley assign them to
the Trenton stage, and Ami is inclined to regard them as lying
below the Trenton and above Chazy limestone. Frech recently
cites graptolites of this zone as from the “Utica shale of Nor-
mans kill.”

Such an apparent inability to correlate properly a terrane with
such a rich fauna would seem inconceivable, specially so in a
state which, by the labors of Prof. Hall and of his many followers,
has furnished the standard scale of formations for all America,
were it not for the indescribably folded, tilted and crushed con-
dition of the beds, the one-sided character of the fauna, and the
distribution of the graptolites in thin bands in the otherwise
utterly barren, huge mass of shales and sandstones, which, practi-

This paper was submitted Ap. 1, 1900, to the Boston society of natural
history in competition for the Walker prize, and a synopsis of the same

read before the American association for the advancement of science June
26, 1900.

miles south of Albany. ' spat, an r
ties where fossils were Re before, and a

Abbey (Glenmont). A number of new localities 3 ne
which, by their arrangement in zones and by their fc foss
allow a step forward toward the solution of be!

justify the present publication, par

HISTORY OF THE HUDSON RIVER BEDS

The history of the problem of the Hudson river beds h hi a wt
treated, though only in regard to the validity of the n
James Hall (17) and C. D. Walcott (36a), to whose pape
reader may be referred here.

W. W. Mather

The term “ Hudson river slate group” was proposed in =,
by Mather, in his annual report on the geology of the first oe os *
trict (1), where he says (p. 212): “ (1) The lowest in the series [of a 1g
fossiliferous rocks] is the Hudson river slate group, consisting of am
slates, shales and grits, with interstratified limestones, all of r a
which occur under various modifications. This group is overlaid
unconformably in many places by the various rock formations of cet ~
more recent origin.” The following fossils (graptolites) are men- i
tioned besides a few shells: “Fucoides gs erra, F. den-
‘atus, and two other species which are probably F. line-

atus and F. ramulosus”,

San ee. ee
‘See References, p. 581.

~
4 > ge a
5 -
OD ] = 7
~¢ a ae
a wt ay

st rata, of. ie udeon river group in ibe sotheat Ce a
ling Albany county) are described under two heads (p. 875):
se east of the anticlinal axis, which are upturned.

se west of the anticlinal axis which are but little dis-

The anticlinal axis above referred to ranges from near New
altimore by Saratoga lake to Bakers falls. —
- Of the upturned strata it is said that they all dip
eastsoutheast, and in regard to the less disturbed beds
; ‘Dr Mather remarks (p. 377); “The horizontal and slightly
inclined strata of slates and grits of the Hudson river
group, lying on the west of the anticlinal axis, as traced from New
7 Jersey to Saratoga lake, were formerly considered as more recent
a strata than the upturned rocks of the Hudson valley, and as resting
3 unconformably on them. It was not until the labors of the geo-
logic survey were more than half completed, that sufficient evi-
dence was obtained to establish the fact with certainty that they
are of the same geologic age.” It is farther stated that the strata
/ could be traced across the line of disturbance only in the Mohawk
valley, that however, the Trenton and the Utica formations were
recognized in the tilted strata by their fossils, the Utica shale by
the graptolites.

It follows from these quotations that Dr Mather distinctly cor-
related the Hudson river beds with the Lorraine beds, or rather
with the Frankfort slates of the Mohawk valley, that he farther
believed that the Trenton and Utica beds could be recognized
in the Hudson valley. As to the latter, it is evident from his
description of the Utica slate that he did not yet discern between
the Normans kill graptolites and the Utica shale graptolites and
considered all graptolite-bearing shales as being of Utica age;

Ps
i

@+) sa ny Y 4 ‘ : i y
_ Normans kill sh
7 rs we 2 nag Ay ee x 7

( ’

ch ee ay
: eae eh a oral: Ae Tarte Van a 2
Taidaae Vanuxem (5), 1i aii of t a ds
cepted Mather’s term and called all pores between |
shale and the gray sandstone of Oswego, the Hudson
but pointed out, that there are two divisions vite ha
tensive, embraced by this term, namely, a lower a er
fort slates) which passes from the Hudson valley th’ rough:
Mohawk valley and extends north by Rome through eee
into Jefferson county; and an upper division (the Pulaski aa
which first appears in Oneida county and extends from th
north and west. Fossils are rare in the Frankfort. slate, b
numerous where it joins the next series, the Pulaski ae hey —
have been reported from near Rome, Westmoreland and Ut ce wi
and also from Cohoes near Waterford, though the species are 1
enumerated. we

It is obvious that Vanuxem correlates only the lower or re
fort slates with the beds of the Hudson valley.

Ebenezer Emmons

In the same year Dr Emmons (3) described shales of the Hudson |
valley as the Hudson river series or group and stated their exten-
sion northward through New York and Vermont to Quebec and
through Pennsylvania into the southern states. He proposed the “ig
mime “Lorraine shales” in place of the names “ Pulaski shale” :
and ‘‘ Hudson river shale,” used before, on the ground that at
Lorraine alone a complete section with the top and bottom of
the group exposed, could be found (3:119). This term has

since been struggling for ascendancy with the term, Hudson river
bede.

Pare es caused eects by the finding of Frankfort slate
fossils (Modiolopsis nuculiformis, Cleidopho-
rus planulatus, Lyrodesma pulchella, Mur-
-chisonia’ gracilis, Carinaropsis7 patelli-

formis, C..orbieulatus, Bellerophon cancel-
Jatus), and of Ambonychia radiata, which is
characteristic of Vanuxem’s upper division, in the Hud-
son river shales of Waterford (see localities of these
fossils in y. 1, Pal. N. Y.) These fossils seem, indeed, to
connect the western fauna with that of the Normans kill beds,
but it may be remarked here that the writer has obtained evi-
dence showing that these mollusks nowhere occur in the same
beds with the Normans kill graptolites, but in actual Lorraine
beds which are stratigraphically widely separated from the grap-
tolite beds. That Hall himself did not feel sure of his correla-
tion becomes evident from an interesting footnote on page 829
of the above cited fundamental work.

This uncertainty may also explain why in the third volume
of the Paleontology of New York (8: 14), Hall extended the term
Hudson river group to “all the beds from the Trenton limestone
to the Shawangunk conglomerate,” an extension of the term

worth and, interestingly enough, with s simila 7
paper of Billings’s is indicative of the complete
correlation of the Hudson river shales which ae out
was wrought by the influence of the Canadian sur
influenced by the presence of primordial fossils int ie Av
valley region, assumed that the oldér rocks of Canada a ind ¢
Champlain valley extended into the Hudson valley. Th i.
ence of Emmons, who had extended the term, Taconic, t
shales of the Hudson valley and asserted the continuation o
Hudson river shales to the primordial region of Quebec, 1
powerful in shaping Hall’s view of the older Lower =a ic a
of the Hudson river shales. When Hall received the g ap oli es
of the Canadian survey for description, and believed that he
nized in species from Point Léyvis and other localities on 5
St Lawrence below Quebec, Normans kill species, he came a
openly (10) for the “ primordial (Quebec) age.” of the bulk of = oF
the Hudson river beds, assuming with Logan, that the two se aes
three occurrences of a few fossils of the “second fauna” were
“outliers of insignificant extent embraced within the folds of — ee,
the older rocks or resting upon these primordial beds which
formed the fundamental rocks of the valley, and that the de-
ranged and altered Hudson river beds were separated from the
unaltered beds in the west by a fault”. He, therefore, dropped
the term Hudson river group, stating expressly (10:444) that
the graptolites of the Hudson valley do not belong to the second

fauna, but * hold a lower position and belong to the great mass
of the shales below”.

Jk ser rir

ie

eras ee to sr aeemicie ah ane ‘doubt
3 relation, and Nei ise in 1877, an read a neve (Lz)

donee fiat: within the limits indicated, all ibe fossils were of

the second fauna, ‘Many of the species of graptolites, so abun-

dant in certain localities of the disturbed and partly altered
shales, were also found in the shales and sandstones which gradu-
ally assumed an undisturbed and unaltered condition within a few
miles west of the river, extending thence through the Mohawk

valley, where they rest conformably upon the limestones of the

_ Trenton group.

With this declaration Hall returned to his former view of the
continuity of the graptolite-bearing beds of the Hudson river

| shales with the Frankfort slates of the Mohawk valley and the

Lorraine beds of the northwestern region. It is a misfortune
that he does not specify the many species of graptolites which he
says are common to the altered shales of the Hudson valley and

to the more western undisturbed beds, as this observation forms

the principal base of his correlation and has not been verified
by other observers, while it disagrees with the writer’s results
on the distribution of the Normans kill fauna to the west of the
Hudson valley.

The cause of the misinterpretation of the rocks of the Hudson
valley is, in the same address (17:261), very appropriately at-
tributed to the “fact, that not only the rocks in the immediate
valley of the Hudson, but also those between the river and the
eastern limit of the state, were treated as a single group or sys-

7p

se Group by eaten ee
certain extent, committed a similar error by uni
and Normans kill faunas in one group, for this co
will be shown still farther on, the principal cau

troversy in regard to the age of the Hudson river gi

R. P. Whitfield eek:

The composite character of the Hudson river beds was first p

tively asserted by R. P. Whitfield in a letter written in 1875 to]

C. A. White (16). Prof. Whitfield’s most important stater
in regard to our investigation are:

From the evidence furnished by these fossils (graptoli 28) da
have reached the conclusion that the graptolite-bearing— a c
there are of the age of the Utica slate, the following being a su i
mary of the facts I have observed. OAT

I have found the following species common to both the grapto
lite layers at Normans kill and those of'the Utica slate formation =
at the mouth of Oxtungo creek near Fort Plain N. ¥.:Grapto- be a 2
lithus (Monograptus) serratulus, Hall, G. (Dip-
lograptus) pristis, Hall (not Hisinger), G. (Clima-
cograptus) bicornis, Hall and G (Dicranograp-
tus) ramosus, Hall.

Just south of Troy, in the shaly partings between layers of ve me
metamorphic limestone, I haye found a species of graptolite in
great abundance indistinguishable from G. amplexicaulis
Hall from the Trenton limestone of Herkimer county, N. ¥,
The same species was also found abundantly in the yard of the
arsenal at Watervliet by Capt. C. E. Dutton, U. 8. A.

From the foregoing facts I infer that the slates below Troy and
in the arsenal yard, together with the associated metamorphie
limestones, are the equivalents of the Trenton limestone.

*
*. aw
ee

ni

= tans “a <a

HUDSON RIVER BEDS NEAR ALBANY 497

The most interesting discovery of Whitfield’s is that of the
presence of shales of Trenton age among the shales of the Hudson
valley. The writer has carefully compared specimens of the grap-
tolite in question found at the arsenal yard and preserved in the
state museum with the D. amplexicaulis found in the
Trenton limestone at Middleville and is convinced of their iden-
tity. Besides this graptolite other fossils have been found in the

_ shales and calcareous sandstones (not limestone) of south Troy

and the neighborhood of the arsenal which more firmly establish
Prof. Whitfield’s discovery.

The supposed homotaxy of the Normans kill fauna with that
of the Utica shale is based on the occurrence of four graptolites
in both faunas. Of these the presence of Didymograptus
serratulus in the Utica beds has not been verified by other
collectors and is doubted by Lapworth and Gurley; Hall’s
Diplograptus pristis, however, is partly identical with
Hall’s D. quadrimucronatus, which is very common at
Fort Plain as everywhere in the Utica shale, and which at that
time was considered also by Hall as occurring only at the locality
from which it was first made known (Lake St John, Canada),
and partly identical with Diplograptus foliaceus,
Murchison.

The two forms, D. foliaceus and D. quadrimu-
cronatus, are not always easy of separation, when com-
pletely flattened in the shales; and the writer also has, follow-
ing Hall’s example and identification,*described colonies of D.
quadrimucronatus as belonging to D. pristis Hall.
Fritz Frech (54:626) supposes this large mucronate form of the
Utica shale to be D. whitfieldi, Hall. A detailed account of
all these forms will be given by the writer in another paper.

Climacograptus bicornis and Dicranograp-
tus ramosgus are, indeed, common to the Normans kill and

1Diplograptus quadrimucronatus Pe otad to the Utica

shale, and for this reason, can not be adduced as connecting the Utica and
Normans kill shales; Diplograptus foliaceus, which is more
common in the Normans kill shale, ranges from the Chazy to the Lorraine

beds and hence is of no taxonomic value.

=o U tic “ oe on § al

of Dix Stites nd Climacograptid:
scien loipsean Gar eeu leci ely yo er
than the Normans kill fauna, an becomes ap parer i a a
son with the vertical range of the same forms in Sweden
Great Britain. In fact, to the time of his death EF in iste
the different age of the two faunas, as the orien is
personal information from the genial paleontologist.

The concurrence of the two graptolites will indicate |
more than the Middle Champlainic (Siluric) or Mohawkian Pe
the Normans kill beds. es a

The Cohoes beds which Whitfield believes to be of ou
with the Normans kill beds are homotaxial with the air
beds, as already suggested by the Trinucleus co nee
tricus collected in them by Whitfield. They are evidenthyal
same beds from which Hall reports such typical Lorraine fos: ils ans
as Ambonyehia radiata and in which also the wate
has found an undoubted Lorraine fauna. In regard to the Lor- —
raine beds, however, which Whitfield supposes to occur close to :
the Normans kill graptolite beds along the Normans kill, the om
writer has not been able to obtain any data, but he believes the
small Diplograptus on which Whitfield principally bases
his correlation to be the Diplograptus putillus of the
Utica shale, which has been found by the writer in several locali-
ties farther up the Normans kill.

ae

C. D. Walcott
Four years later, in a paper read before the Albany institute
by ©. D. Walcott (36a), the Normans kill beds were included in
the Utica slate (as “Utica slate 2”—see the catalogue of fossils,

: nae ae Sasa of me equivalency of he graptoitie slates sn
tica slate, is also cited, pest
( citations prove, Walcott based ee correlation on the 5 .
lity of the shales of the Mohawk valley with those of the Me:
n valley and on the Utica slate localities in the Hudson cs
y as mentioned by Mather, and finally on Whitfield’s asser- |

oe

‘he first argument has been meanwhile weakened by the estab-
lishment of the presence of a fault between the disturbed and
__ undisturbed regions, which was already assumed by Emmons,
ee and will be spoken of farther on (p. 504). Mather’s assertion
of the presence of a zone of Utica shale localities in the Hudson

valley was caused, as shown above, by his failure to distinguish

between the Normans kill and Utica shale graptolites; and Whit-

field’s correlation has just been discussed on the preceding pages.

T. N. Dale

In the same year T. Nelson Dale (20) discovered in an outcrop
of argillaceous schist about a mile west of the Hudson opposite
Poughkeepsie, crinoid stems, Orthis testudinaria, O.
pectinella, Leptaena sericea, Strophomena
alternata, Bythotrephis subnodosa and a cast of
a gastropod which resembles Bellerophon bilobatus
(all being Hall’s identification), some of these fossils being also

‘found near Vassar college and south of Poughkeepsie.
The author concludes from his determinations that “ the clay
slates and shales in the vicinity of Poughkeepsie, on both sides
of the river, are fossiliferous and that they very probably belong

aia a as Ne PDR, re |
ie ta BelieronD emt See ee ee
"curring from the Trento ae Serer a a

trephis paeese cna seing a rather indis Dp
ment, is of little or no taxonomic value, Ort this peeth ij
is declared by Hall himself (7:128) to occur in ne
part of the Trenton limestone, though unknown to I him in
Hudson river group. Theodore G. White, in his roe
paper (51:83, 94), reports the form only from a six fe a
overlying the Black river limestone of the Poland limel in
tion. In the Cincinnati region and in Canada the fossil is fi
in the Black river and Trenton beds, and Winchell and Ul
announce it in their carefully prepared lists only from the 1 ap}
Black river beds of Minnesota (49), ai ak

The evidence afforded by the fossils of Poughkeepsie neni 8
then rather indicate for these Hudson river schists the age o
Trenton limestone.

J. D. Dana and W. B. Dwight

At the same time the problem of the Hudson river shales was _
approached from the east by James D. Dana (21), who found
that the five limestone belts traversing the schists east of the
Hudson river are anticlines of limestones, underlying the schists.
He also succeeded in finding fossils in the limestones which were
described by W. B. Dwight (23), as denoting a Trenton fauna.
Dana, therefore, concluded that the “Taconic schists ” overlying
the limestone are of Hudson river age.

Dwight cites the following fossils: Orthis tricenari a,
O. pe c tinella, O. testudinaria, Leptaena seri-

See
‘Dana hi 1d meanwhile (Manual of geology. 1874) proposed to unite the

Trenton, Utica and Cincinnati (= Lorraine) epochs under the term Trenton ;
period.

; J *
%

re; pectinella, Rhynchonella capax, Leptaena
sericea, Strophomena alternata, a new Discina
~ (later described as D. conica); Chaetetes compacta,
very abundant, Ch. lycoperdon var. ramosus, Schi-
zocrinus nodosus, Echino-encrinites anati-
formis, probably O. tricenaria, and Petraia corni-

culum.

The author adds: “ These developments establish this beyond
doubt as a stratum of the Trenton limestone”. A farther
conclusion which could be drawn, is that these faunas contain
no forms characteristic of or restricted to the upper Trenton,

while they distinctly point to a lower and perhaps in some de-

gree middle Trenton age for the beds; for Orthis tricen-
ariaandPetraia corniculumare restricted to the lower
Trenton, Illaenus crassicauda occurs in the upper Low-
ville and Trenton limestone, Schizocrinus nodosus is
most abundant in the lower Trenton, Ptilodictya acuta
and Escharopora recta occur only in the lower and cen-
tral part of the Trenton, Echino-encrinites anati-
formis is a middle Trenton form, and the abundant Chae-
tetescompacta is restricted to the Black river.

sd aga bivornis, Dierkkonenion
Diplograptus mucronatus, rae ems,
tis terminalis, Leptaena sericea eee
Orthis testudinaria, Zygospira modes
icula trentonensis, Cleidophorus pla ul
Ambonychia undulata, Tellinomya ¢ li
levata, Lyrodesma poststriatum, 10 m |
mined species of lamellibranchiata, Hy olithes am
catus, H. sp.?, Bellerophon bilobatus, B. «
cellatus, Murchisonia_ gracilis, Ende ce
proteiforme, Orthoceras bilineatum?, ©
ulitesflexuosus, Plumulites sp.?, Triar thr
becki, Trinucleusconcentricus. | es
Beecher referred this fauna to the Utica epoch, and Wale ot iar .
(36a : 345) later declared it to be “as a whole, characte ristic q o
of the upper portion of the Utica shale in the Mohawk alley |
and of the passage beds between the Utica shale zone and the”
lower portion of the Lorraine shales in the section at as
Jefferson co. N. Y.” ee aa
The import of this discovery is that it establishes the hitherto
only suspected presence of the Utica shale among the shales of |
the Hudson valley, but it does not warrant the conclusion of
the Utica age of the Normans kill graptolite fauna, for of the
three graptolites found by Beecher, two, Climacograptus
bicornis and Dicranograptus ramosus, are com-
mon to both the Normans kill and Utica faunas, and the third,

Van: oe
j We SA fe 3

Sa «
a, aa 2 ths

ates, was found. This yielded the following species:

Asaphus platycephalus, Calymene senaria,
- Orthis testudinaria, O.lynx,Leptaena sericea,
S$trophomena alternata and the hemispheric form of

Chaetetes lycoperdon. He concluded: “ None of the

species of this locality are distinctive of the Utica slate, and both
the limestone and its associated graptolitic slates represent in my
estimation the Hudson river group.” These fossils are, however,
not restricted to the Hudson river group and would prove only
that the Normans kill graptolite shales may belong anywhere
from the base of the Trenton to the Lorraine beds.

In another paper (30), Ford discussed the age of the slaty and
arenaceous rocks in the vicinity of Schenectady, which by Mather,
Emmons and Whitfield have been considered to be of Lorraine
age. Ford found at Schenectady Graptolithus pristis,
Gr.mucronatus (that is, a mucronate Diplograptus),
Triarthrus becki and a Lingula, which he considers
to be Lingulacurta. On the strength of this evidence he
regards the Schenectady beds as of Utica age. This result, if
farther verified, would be interesting in so far as it would show

bany and gcneneateds: and to be raat in ie ffects ;

south as Kingston.” The demonstration of this break b
the tilted strata of the Hudson river region and the ur dis
beds of the Mohawk valley is of great importance for our i nv v
gation, as it refutes the argument presented by Mather, F al I:
Walcott, that the Hudson river beds of the Hudson river res
are continuous with and can be traced along the pares
to the Utica and Lorraine beds of that valley. As the ,
branchs, cited by Hall from Cohoes, and other fossils foun a
the writer at the same locality (see farther on) prove, the
raine formation is well represented at the lower Mohawk, :
on the western side of the fault, the Utica shale, as claimed by ‘" RE
Ford, may be found. Hence there is no continuity along the lower — oss |
Mohawk. Similarity of lithologic characters can, in the great = on
mass of similar argillaceous shales, arenaceous shales, sand-
stones, grits and argillites, representing the Hudson river series
of beds in the Hudson valley, only, if ever, be relied on in dis-
tinguishing the formations after the most minute study of these
lithologic characters. The description of the localities in an-
other part of this paper will bear out this statement.

ee

.
cam D

N. H. Darton

The same fruitful year brought out another discovery of fos-
sils in the Hudson river shales, that by Nelson H. Darton
(32) near Sugar Loaf, 21 miles southwest of Newburgh and at

TN et

I, P. Bishop

od While thus the fortunate discoverics of fossils other than grap-

~ tolites in the “ Hudson river shales” began to furnish evidence
of the Trenton age of part of the shales, other investigations,
notably those of I. P. Bishop (33) tended to demonstrate the close
stratigraphic relationship of the Trenton limestone and the grap-
tolite-bearing Hudson river shales; for, in Columbia county, it
was established by Bishop that “ the limestone containing Tren-

ton fossils immediately undérlies the graptolite shales of the Hud-

son river group”.
; Charles Lapworth .

An entirely new course to the solution of the problem of the
age of the Normans kill fauna was entered on by Charles Lap-
worth (34), who studied the graptolite faunas from numerous
localities in Canada, and sought to determine their age by com-
paring them with the faunas of the detailed graptolite zones which
he had so well succeeded in establishing in Great Britain. A
farther innovation in the mode of viewing the problem is implied
in Lapworth's suggestion that the Normans kill graptolite beds
do not necessarily represent a separate stage in the series of forma-
tions but are probably equivalent with certain calcareous strata

pa
ie i
»

“Np a L .
oe no question of the general
Re ee Lae Coenogra sO ints
ees TSt T
y Sy Se , ‘

I

vt

‘sola have slwasa adueree Geet at. ormé
Deda are ofthe age ofthe Hudson siver group (E ‘ine) or
of the Utica slate. 5
But here we have to recollect that, with eu exe :
field’s distinct assertion that G. serratulus, |
the Utica slate of Oxtungo creek—which may be e ccou
for on the supposition that what Whitfield calls a “Da i ¢ ‘dyn
graptus may possibly be a Le ptograptus—not a shat
of paleontologic evidence has yet been adduced to show thé att
Normans kill or Marsouin rocks are newer than the Trenton. —
I will not discuss the evidence further in this place, bu ut
merely say that in Great Britain the fossils of the Coenograptt
(Normans kill) zones occur in the beds immediately st eng
the typical Llandeilo limestone of Wales, with O gygi
buchiiand Asaphus tyrannus, and in association wi
the Craighead (Stinchar) limestone of Seotland, with Maclur
loganiandOphileta compacta, i.e. in beds apparently
homotaxeous with the Chazy or lowest Trenton (Birdseye and
Black river). a
If, therefore, we provisionally regard this Normans kill (Mar-
souin and Griffin’s Cove) zone as coming between the Chazy
(Maclurea) and the Trenton limestone in America, it will
answer roughly to its equivalent, the Coenograptus gracilis zone
in Great Britain, in age as well as in fossils.
We must remember that they appertain, possibly, almost to
the very lowest beds of that second fauna, i. e. their place is
practically Trenton-Utica, and not Utica~Hudson.

E. 0. Ulrich

FE. O. Ulrich cited some Normans kill graptolites from the Utica ea
shale of Cincinnati (35:183). As these have not been mentioned
in later lists of fossils (49), it is probable that they have mean-
while been differently determined, and that the Normans kill zone
is not represented in the regions studied by him.

i .
x very ae ‘aigtuebed ae a at a high rick In this
the noted cecal beds of Normans kill occur; also

a - shales and sandstones which, at the Indian Ladder, were found
to contain Orthis testudinaria and Trinucleus
ee oncentricus, are correlated with the Frankfort shales of
AB the Mohawk valley. Mr Walcott’s conclusions of the presence
of a zone of Utica shales in the Hudson river valley and of the
5 extension of the Frankfort shales along the Normans kill are
___— mainly based on lithologic evidence. Fossils found at numerous
| localities by the writer have served to verify the former conclu-
sion; while Utica shale fossils found on both sides of the line
of disturbance at the Normans kill indicate the presence of
faunistic differences in the shales and sandstones, in spite of their
apparent lithologic continuity.

The relation of the Normans kill, or Coenograptus, zone to the
Utica shale is not expressly stated by the author, but it is
clear that he places it near the top of the Utica shale. This
follows from the following statement (p. 349): “‘ Comparing the
fauna, we find that the forms of the upper part alone of the Utica
zone occur within the valley of the Hudson, and that the great
graptolitic fauna of the Hudson valley is largely unknown in the

formation is knows from the annie of “Waterford, a “a
upper part of the former or the lower part of the lat
Normans kill fauna is to be placed. | *

In accordance with this conception of the divisions of the H
son river shales and sandstones in the Hudson river B: y;
term “ Hudson” was proposed “ for the series of shales betw
the Trenton limestone and the superjacent Upper Siluriar ir -ock

In the discussion following the reading of this paper Prof. H
expressed his full concurrence with the results obtained
Walcott.

H. M. Ami —

It is an interesting fact that, as seen again from this paper,
whenever the New York geologists had occasion to assign the "
Normans kill zone in the series of the New York rocks, they gave’ a.
it a position within or above the Utica terrane, while the geolo-
gists who were studying the fauna of the same zone in Canada,
Billings, Logan and Lapworth, invariably placed it below the
Utica shale. This attitude of the two schools is still more em-
phasized by the next student of the graptolite faunas of Canada, =4
Henry M. Ami (38). :

Ami makes the following interesting remarks:

sefore assigning a definite position to the rocks of Quebec city “4
in the scale of terranes in America, it is necessary for the writer
to state that so far he has been unable to find any evidence in

the field, either stratigraphie or paleontologic, whereby the
Hudson river rocks and Lorraine shales , as originally understood

ae which has pees yet ee fi und either in

1U yerous places the name “ Hudson river ” e.g. at Normans
1 and many other localities in New York and Vermont, and in
in da. Similar pancase have also been observed in northern

5 “The apparently ont Trenton aspect of a portion of the Que-
165 bec massif as seen at Cote d’ Abraham and Cote de la Négresse
in gives us an indication of the age of the strata at these points.
i f _ Cut off on all sides by’ faults and separated from the Lévis rocks
_by the St Lawrence river, the Quebec terrane (which name I beg
to propose for this series of strata such as we meet at the Mont-
calm market, Parliament square, and drill shed exposures) stands
by itself in an anomalous position very similar to rocks of similar
age which Prof. Lapworth designated as “unplaced in the series”.
The presence of such forms as Agnostus, Aeglina,
Ampyx,Dionide, Bathyurus, etc. points to a rather
low[er] horizon than the Trenton, while I believe that it is per-
haps premature to give the precise geologic position of the strata

at Quebec, in the present light of our knowledge.

In the discussion which followed the reading of this important
contribution to our knowledge of the Champlainic [Lower Sil-
uric] terranes, Mr Walcott expressed the opinion, that, “if Mr
Ami’s determination of the fauna is correct, the horizon of the
Quebec city rocks is that of the Trenton, probably the lower
Trenton, and perhaps the upper portion of the Chazy of the New
York section ”’.

The writer concurs with Lapworth and Ami in considering the
Normans kill or Marsouin zone as “a distinct development of the
Ordovician ”, which view is supported by evidence obtained
around Albany, and also with Walcott in so far as he considers
the horizon of the Quebec city rocks as that of the lower Trenton.

Moordener. kill, partly below an Aomiaane’ ‘ill sh
embedded in them, a conglomerate full of
ton fossils, in matrix and pebbles, and ieee 1
merous specimens of Ampyx and Remopleur: id
And in Europe, notably in Sweden, the above me —_
genera ascend into and above horizons considered as |

otaxial with the Normans kill and Utica shales. A gn: 10
tus and Ampyx occur in the Trinucleus shales — ¥
Sweden, Ampyx tetragonus even in the upper part 0 ft =
middle graptolite shales; and Dionide is an important genv
of the Trinucleus shales, where also Aeglina still oe eu
Bathyurus is still well represented in the Trenton of Amer- ; Hi
ica by forms like Bathyurus extans,spiniger and
schucherti. The occurrence of these genera in the queasy
beds is, in the writer’s opinion, an interesting proof of the Euro-
pean and Atlantie connections of the Normans kill fauna already
indicated by the distribution of these graptolites which oceur
only in Europe and to the east of the Appalachian region, west
of the Mississippi valley and in the far northwest, etc.; while the
Trenton fauna has all the characters of an epicontinental fauna,
restricted to the American continent and progressively developed
by a sudden transgression of the sea. The retention of these an-
cient trilobite genera in the graptolite facies of the Trenton is
then only an interesting instance of the retarded development of

the oceanic fauna in contrast to the progressive development of
the epicontinental faunas; relations which lately have been so 3
well elucidated by Chamberlin (59) and Weller (60). These facial

ica , OF vice versa”. This Tnieronre stands in accord with
rorth's conclusion of the parallelism of the graptolite faunas
Ss supports his correlation of the Normans kill zone with the
es ~ lower ‘Trenton on the base of such parallelism. Dr Gurley also
asserts the lower Trenton age of this zone, which he terms the
Lower Dicellograptus zone.’

/
.

| T. N. Dale

Shortly after the completion of the present paper a most
elaborate account of the slate formation in the region to the
northeast of the investigated territory, by T. Nelson Dale (63)
came to hand. Mr Dale’s views in regard to the age of the Hud-
son river beds agree in a gratifying manner with the results to
which the writer was led by. his own observations. In the slate
belt, which extends northward from, the Hoosac river in eastern
New York and in Vermont for about 55 miles, the Cambrian
slates are in some localities followed by Calciferous shales, with
Calciferous graptolites and thin limestone beds, but in more lo-
calities they are overlaid by various other Champlainic [Lower
Siluric] rocks which are described as Hudson grits, Hudson

|

1The upper Dicellograptus zone is Lapworth’s zone without Coeno-
graptus gracilis, in which, however, subsequently a Coeno-
graptus has been found by Ami, and which has not yet been clearly
differentiated in the Hudson river valley.

iat peeled ative ni uae se ss a] pear to be replac
the strike by the red and green Ordovician slate ” ( ‘(p. 18:
The Trenton limestone (p. 190) occurs rs only. spo orad. oe
the lower Siluric areas. “In some places it wa
posited contemporaneously with the Hudson —— sha
it may underlie portions of them. In others it may = ore se
entire Lower Silurian series and should then be regarde
Trenton, Chazy and Calciferous.” te $
This correlation of the Trenton limestone and the Hu¢ son ri
beds is also expressed in the table of formations (p. ‘aan
it is said: “Trenton limestone: Limestone, occurring mo a 3
west of the slate belt, replacing probably I (Hudson grits, red a in a .
green slate and graptolite shales), H (Hudson white beds a
Hudson thin quartzite) and G (Hudson shales), and psig F e

(Calciferous) and then representing the Trenton, Chazy and Cal- —
ciferous.”

RESULT OF FORMER INVESTIGATIONS

A brief retrospect of the opinions expressed by the various
authors on the Normans kill fauna will show that there has been
a decided trend in these opinions toward a correlation of the Nor-
mans kill zone with deeper and deeper terranes till now it os-
cillates, so to say, about the lower Trenton. This correlation is
based entirely on paleontologic evidence and, as Dr Gurley’s con- - |
cise statement clearly shows, is hardly more than tentative. This,
however, can not be surprising, when it is borne in mind, that
all the graptolite beds in New York, notably those at Normans
kill, the Abbey (Glenmont), Schodack Landing, Kinderhook and

udson river Ue shlene that the wks presents-his observations

1 this problem in an area which appears insignificant in com-

vison with the great geographic extension of the beds in ques-

tion. But only by restriction to a definite small territory has it
been possible to visit every outcrop and, what is still more im-
portant, to collect in every outcrop most exhaustively and min-
- utely. As a gratifying result of this method, there were found in

the region described in the introduction, 29 localities which fur-
nished fossils. These, with 7 localities known before, give 36 sta-
tions with fossils. These can be arranged according to their fos-
sil contents in four zones, which, following the general strike
of about n 20° e of the rocks in this part of the Hudson river
valley, extend from n n e to s s w. The stations will be
described according to these zones (see map).

DESCRIPTION OF STATIONS

A LORRAINE BEDS
Station 1. Cohoes falls of the Mohawk river

All along the lower Mohawk and specially from the high falls
of the river at Cohoes to the islands in the Hudson river opposite
the mouth of the Mohawk, is exposed an enormous mass of
greatly contorted rocks (a sketch of these contortions is given by
Mather, 4, pl. 2, fig. 1) of mostly shaly character; that is argil-

ohity ie ellandiag ia foe 1suz ;
opening of ditches for the purpose 0

at

sear’ the Mulawk. Gade! at Mark vce shales, ch:
through dark sandy shales into pepe cgenie :
into. They furnished:

Glyptocrinus decadactylus, Hall, numerous joint?
Diplograptus putillus, Hall, several specimens! |

*This small form was originally described by Hall (11:44) 1
“ Hudson river group of Iowa ”, and is also cited by Schuchert f
“Hudson river group” near Granger and near Springvalley M
from Graf Ia. One of Hall’s types is reported in Whitfield & ] vey
catalogue (61) to have come from Dubuque Ia. According to— a ey
lists the form is restricted to the Utica horizon (lower Maquoketa gs Pie
Sardeson (57) distinguishes the lower Maquoketa formation as “ Diplo- =
graptus-bed”’, Though he doesnot give any identification of the Dip: -
graptus, it becomes apparent from the localities of this horizon, mentioned ss iy
by him (Graf Ia. and Granger Minn.) that Hall’s and Schuchert’s —
specimens were also obtained from this horizon. The writer’s observations 2
on the vertical range of this form in the east agree well with these data;
for D. putillus has been found to be common in the Utica shale of cer-

r pet
tain parts of the Mohawk valley, specially north of Utica and near the %
Village of Mohawk; and I have recently found it in great abundance, =a
together with Orthograptus quadrimucronatus, Cory- a
noides curtus anda minute, undescribed spinous Diplograp- ‘a

tus, in the Utica shales directly above the Trenton limestone in the
beautiful section along the shore of Lake Champlain near Panton Yt., to
which interesting locality the writer’s attention was kindly directed by
Dr Theodore White of Columbia university. |

The form may, howey er, as its occurrence at Waterford proves, pass
into the Lorraine beds.

J acer zones : and is the only species of Cor ynoides
by him and Dr Gurley from America. It is also very common
2 Normans kill shale, and was figured by Hall among the “ germs”,
: ntly on account of its similarity with the sicula (Decade 2, pl. B,
19; 20th mus. rep’t, pl. 1, fig. 19; Pal. N. Y., 3:508, fig. 7). While
ynoides calicularis is apparently restricted to the Dicello-
ptus zones, and did not continue to live into Utica time, another form,

ee _ only half as long, much stouter and agreeing with the figure of Cory-
- moides curtus, given by Lapworth (Armstrong, Young, and Robert-
gon, Catalogue of West Scottish fossils. 1876. pl. 2, fig. 92) has been
found to replace the longer form in the Utica beds of Panton Vt., the
‘Rural cemetery of Albany and other localities in the Hudson valley, while

specimens in the collection of the New York state museum prove its pres-

ence also in the Utica shale of Amsterdam. One slab from this locality is

so densely covered with these graptolites that hardly any interspaces are
left; on another slab from the same locality they lie associated with

Peaplosraptuas putillus, Lingula curta and: Lepto-

bolus insignis. One slab of typical black Utica shale from Sprak-
ers Basin shows the same fossil. It is a remarkable circumstance that
the writer has never seen a single specimen in the Utica shale of the
middle or upper Mohawk valley, nor are there any specimens in the rich
Rust collection of the state museum from Holland Patent. This may
indicate a regional difference in the fauna of the Utica shale. The com-
mon occurrence of this fossil in the sandy shales of Waterford, whence
the writer has it in the same slabs with Trinucleus concen-
tricus and the lamellibranchs of that locality, proves that it even
ascends into the Lorraine beds. One specimen has been found at Cal-
lanan’s quarry near South Bethlehem in the shale of that formation 15
feet below the waterlime bed of the Upper Siluric.

The writer has obtained such a good representation of this still very im-
perfectly understood form (Frech cites it among the doubtful forms, 54:
580), that its more important morphologic characters can be made out,
and will be published in another place.

p20 AE oO, tery AS) DAS

ie Green ms rgnee’ PO om
Trinucleus concentriens, pei emacs. ae os
This fauna is undoubtedly, as determined ?
representative of the Lorraine fauna, } or more €:
out by Walcott, of the lower division of the I
the Frankfort slates.

ne Hall
par

Station 2. Block island, Cohoes’

Another typical Lorraine fauna was found a little far he
east on Block island, a picturesque steep cliff rising ;
rocky bed of the northern branch of the Mohawk stint Co oh =
Along the eastern wall, besides graptolite shales with fy > lo-
graptus foliaceus and a few specimens of D. putall r |
a stratum of fossiliferous mudstone is exposed over a cc isider-
able area. This furnished: Sa

Heterocrinus heterodactylus, Hall. Stems and points, cc

Sagenella sp. on Endoceras. r

Crania sp. r

me

Platystrophia biforata, Schlotheim sp. r

Cyrtolites ornatus, Conrad. e¢

Archinacella patelliformis, Hall sp, Smooth variety, ¢
Modiolopsis faba, Hall. e¢

Modiolopsis ? nuculiformis, Hall. ¢

Cleidophorus planulatus, Hall. ee

Lyrodesma poststriatum, Emmons sp. Lorraine form, ¢
L. pulchellum, Hall. ¢

‘r=rare, rr=very rare, C=common, cc=very common.

ng > outcrop is met with (station 3) along Dry creek, west of
a6 i Island. This creek has formed a deep gorge through a
OL aogeneous mass of soft gray argillaceous shales. In these
eds only a single layer with fossils was found. There were a
few specimens of Corynoides curtus and more abundant
stipes of Diplograptus foliaceus. The writer colors
“if station 3 (Dry creek) as a Lorraine station, as the two graptolites
are of themselves noncommittal, while the beds by their extreme
_ barrenness suggest their Lorraine age and also lie in the strike
of the Cohoes rocks. )

Station 4. South Cohoes

The reconstruction of a sidewalk in south Cohoes brought out
_a considerable mass of rock, which like that of Dry creek (station
3) consisted mostly of compact dark gray to black, argillaceous
shales with very few specimens of Diplograptus foli-
aceus and Corynoides curtus.

a
ae
“Ss
a
¥.
4
..
i
a
yy
4

Other outcrops of Lorraine beds

No outcrops of rocks which by their fossil contents could be
attributed to the Lorraine age were found to the northwest and
west of Albany, as the brooks have nowhere cut through the
heavy drift covering to the bed rocks. This is specially observa-
ble along the northern affluents of the Normans kill. The next
outcrops occur along the Vly, a southern tributary of the Nor-

mans kill, at the sawmill below Voorheesville, 7 miles west of

= es he 4 * =
7 ri a ott, - >”
- se hae:
Of? © ee 2s >

<, ae a :
ance of ik“. eg — a
fj q

ce of the

can with BP ey. - det ree of certaint
beds. Furthermore, Utica Pah ste (seed
were found in underlying rocks farther down th the cree a |
shining gray fissile shales were found on the south b D
Normans kill about a mile above (west) the month of ;
and an excellent exposure of Lorraine beds was m el t
mills, 11 miles west of Albany, where gray sandstc one ba
feet and more in thickness with intercalated shales,
river. ;
South of this neighborhood, at the Indian Ladder, the In
beds underlie the Manlius limestone, and yielded D aint
la testudinaria and Trinucleus concen' tr .
as reported by Walcott. Other outcrops of Lorraine beds ce
observed at several places along the foot of the He de “Shee
mountains. One of the best of these is that along Sprayt kill :
at South Bethlehem, where, below the railroad bridge, some es :
feet of sandstone causes a waterfall and farther up, at Callanan’s — Bt
road metal quarry, the contact with the Upper Siluric Water-| ts
lime is exposed. Numerous sandstone banks alternate here with ‘
light colored, soft, argillaceous shale and some bands of more bs
sandy shale, In the shale, 18 feet below the Waterlime, a Cory-
noides was found. These beds dip slightly southwest. A very —
coarse sandstone with bluish green mud pebbles is exposed 45°
miles farther south close below the Waterlime and Manlius lime-
stone along the road leading from Ravena to Aquetuck. It
strikes n 60° e and dips 40°, n 150° e, is hence, again involved
in the tilting to the east, characteristic of the Hudson valley re-
gion. It is doubtful whether this sandstone still belongs to the
Lorraine rocks or is already the sandy development of a deeper
terrane. Its strike would carry it far to the east of the Lorraine

~

4
a
i
‘

Ls
—_
bee
eo 4
a
aS
af
j
A

é of the lower Mohawk valley by testing them with HCl,
"sage reagent the ee Utica shale will early ef-

a ane to the shales of the various terranes of the Hudsoa

- valley region near Albany, it was found to fail in the clastic
rocks of this region, where even the Trenton is represented by
argillaceous shales, and among the Utica shales only those from
the penitentiary at Albany were found to effervesce, while all
specimens of Utica shale from various localities of the Mohawk
valley subjected to this test by the writer have strongly reacted.
This indicates the great change in the marine conditions from
west to east in this region throughout a long period.

B- UTICA BEDS

East of this area of Lorraine rocks, the presence of a zone of

- Utica shale extending in the direction of the general strike of

the shales of the Hudson river valley, has been established by
the finding of 15 outcrops which contain Utica shale fossils (Com-
pare the accompanying map).

Station 5. Mechanicsville

The excavation of a large spillway for the establishment of the
Hudson light and power company of Mechanicsville, on the Hud-
son, about 2 miles below Mechanicsville, offered a rare opportunity
for collecting in the shale. Though this locality lies several miles
north of the boundary of the area investigated thus far, it was
thought expedient to include its description in this paper, as the

a

a, roe ‘ i a A
me as at es
a ;

heer

Pee
; paler aoe x,

Dawsonia campanulata, Maden
Pontobdellopsis cometa sp. n2
Lingula curta, Conrad. c |
Leptobolus insignis, Hall. c
Schizocrania filosa, Hall. r
Pholidops subtruncata, Hall. ¢
Plectambonites plicatella, Ulrich. ce
P. sericea, Sowerby sp. ¢ ;
Cyclospira bisuleata, Emmons sp. ec
‘Archinacella patelliformis, Hall sp. ce Me:
Protowarthia cancellata, Hall sp. ‘(=Bellerophon bilo Da tus,
Hall) r ae
Cyrtoceras annulatum, Hall. rr a
Modiolopsis modiolaris, Conrad. r
M. ? nuculiformis, Hall. r
Goniophora carinata, Hall sp. ¢
Cuneamya, sp. fragment. r
Ctenodonta levata, Hall.
Conularia trentonensis, Hall. ¢?

"See p. 574.

*A comparison of this form with the type helen of Conularia
trentonensis, Hall, preserved in the New York state museum, and
with typical material of Conularia hudsonia, Emmons, from the
Lorraine beds, proved that the Utica form, instead of approaching the
Lorraine species by greater coarseness of its sculpture, has, if any dif-
ferent sculpture, a rather closer and finer arrangementof the transversal
and longitudinal lines than even the Trenton form.

” Le a
f c 3
* = @. 4
Ay >.
ad 2 wie
. ae a.
. ats este ae
oS! oa ed a ds
ho J , —. Te ee SS Saul = 2
eee), se. ee ry eo. i

er of eee as well as of ee forms. The Trenton

4 Bem acagraptus caudatus, “Cyclospira bisul-

cata, Cyrtoceras annulatum, Goniophora
_ tarinata, Ctenodonta levata, and Conularia

trentonensis. ,
The Lorraine forms are: Pholidops subtruncata,

Plectambonites plicatella, Modiolopsis mo-
diolaris, Aparchites minutissimus, Cteno-

bolbina ciliata.

anna nnESEIeeS

*The vertical range of this minute but pretty fossil cirriped is worthy of
special notice. It was originally described by Hall and Whitfield (Paleon-
tology of Ohio. 1875. 2:106) from the Hudson river group, Cincinnati O.,
the authors stating however, at the same time, that they had received
from C. D. Walcott “ specimens apparently identical on surfaces of Tren-
ton limestone from near Trenton Falls N. Y.’ This statement can be
verified by the writer, who collected in the Rafinesquina deltoi-
dea beds of Trenton Falls a well preserved specimen. The collections
from the shales of the Hudson valley prove now that it also occurs and is

even most abundant in different horizons of the Utica terrane; for it has

been found besides in the Lorraine beds of Waterford (station 1), in the
upper Utica beds of Green Island (station 10) and of the Dudley observa-
tory (Dr Beecher), in the lower Utica beds of Mechanicsville (station 5) in
great profusion, and in the middle Trenton shales of Port Schuyler (station
23). It therefore persisted, at least in this region, from the middle Trenton
into the Lorraine.

*See descriptions of this and the next species p. 577.

her od =i om

. ‘
a
=
a ia
s

a,

—— pope gs Lo diole
and base nearly pi ao aC

recta, or is ide

tioned | by this author; and a eApari

simus approaches’ the malian var et y by’

subcentral projecting point. a Micke es eat
The Lorraine element is, hence, by no means, so strong y re

sented in this Utica fauna of Mechanicsville as appears
glance or as it is in the Utica shales of Green Island. — Li
still more emphasized by the absence of Cleid oph 1c a
planulatus, Cyrtolites ornatus and Lyrod —
pulchellum, while, on the other hand, the Trenton ¢
is so strong that the beds almost assume the character of t
sitional beds between the Trenton and Utica terranes. __ 5 oy a
An important and novel factor in this fauna is the pe a
Climacograptus caudatus, which occurs f a ly
and in large specimens. This striking type of graptolite struct re +
was first described by Lapworth from the Hartfell shales of Si a Pe :
land which are considered homotaxial with the upper Dicello- _ oy we ne
graptus zone of Canada, from which the same graptolite has been — “f ;
reported. As it is restricted to the upper Dicellograptus nou Te nd
and, therefore, is a valuable index fossil, its occurrence in the | eh
lowest Utica shale of Mechanicsville is of significance, indicating :
the presence of this zone in the Hudson river region and its prox-
imity to the lowest Utica. If we add, that also Dawsonia
campanulata, found at Mechanicsville, and Cry pto-
graptus tricornis, found in similar lower Utica beds on
Van Schaick island (see station 8) are fossils of the Dicellograptus
zones, and not of the Utica horizon, it can be concluded with
some degree of certainty that the upper Dicellograptus zone,
when present in the Hudson river valley, directly underlies the
Utica terrane, that is, is homotaxial with the whole or part of the

Mi,
ae Bona

I blu on the west bank of “fhe e Hudson, |

farth oe north by gray arenaceous and micaceous shales,
in turn underlie alternating sandstones and shales. The

? : ecnivens sp. n. (a oe and numerous hydrorhabds)

Endoceras proteiforme, Hall

Climacograptus typicalis and Diplograp-
tus spinulosus are restricted to the Utica shale, while
Diplograptus putillus finds its ue development
in that terrane.

1Climacograptus typicalis is, according to the consensus of
all writers on the Utica and Normans kill faunas, restricted to the Utica
shale and does not occur in the latter fauna. The only exception is found
in Frech’s statement (54:612) that he has seen specimens of this form
from Normans kill in the Breslau museum. Frech, however, also considers
Cl. parvus a dwarf form of Cl. typicalis, basing this opinion on
a specimen from Cincinnati in the same museum. AsCl. parvus does
not occur at Cincinnati, but is restricted to the Normans kill beds, where
it is one of the most common forms, and as a comparison of these two
graptolites, which nowhere occur together, shows that they can not be
identical, it is probable that he did not recognize the two forms, and his
Cl. typicalis from Normans kill is only a somewhat larger specimen
of Cl. parvus.

Frech also proposes to change Hall’s adjective, “ typicalis”’ to “ typicus ”’
on the ground that the former is an anglicism. While it is true that
typicalis is not a word of classic Latin origin, it was of common usage in
later Latin, and, as many very expressive words have been taken from the
post-classic Latin, it would not be practical to deprive the paleontologic
nomenclature of this source of words by too strict philology.

pact, black, barbamatcons: shales of f them 2 ort lern p
land. The shale contains: Noh Se aoe

Diplograptus foliaceus, Murchison sp. cc
D. putillus, Hall. rv

Cryptograptus tricornis, Carruthers (Dip!
Hall) r

Cameroceras proteiforme, Hall sp. r

ia
Leptobolus insignis, Hall. r ae a ee
Schizocrania filosa, Hall. r “

While the general character of the rock and faunnnk is d distit et]:
that of Utica beds, the occurrence of Crypt ograptus t tr i
cornis is wholly unexpected and difficult of explanatio: ee
this graptolite thus far has been, in America, observed only : as :
member of the upper and lower Dicellograptus faunas, and Bese
Scotland is restricted to the Glenkiln shales, which are homots xial neh
with the Normans kill or lower Dicellograptus shales. The pres

ence of this graptolite points evidently to a position of these beds | an:
at the base of the Utica horizon.

|

. bs MS

Station 9. North shore of Green Island ae

In the bluff along the northern shore of Green Island, directly — fe q
west of the railroad bridge, several fossil-bearing bands were

found in the shales. Two of these were calcareous, and consisted -
almost entirely of valves of brachiopods, a third was a black

compact mudstone, which in one place was highly charged with
fossils. The fossils collected were:

SS ee ee eC CUT

a c
nophorus cancellatus sp. n. ¢
sidophorous planulatus, Hall. cc

oo

ae

+

Ne ee ee a, ee ee

yrodesma poststriatum, Emmons sp. r
eCt,. pulchellum, Hall. c

ie _ Orthoceras tenuitextum, Hall sp. 3

-O. lineolatum, Hall sp. r

Spyroceras bilineatum, Hall sp. c_
Isotelus gigas, De Kay. e¢

Calymmene senaria, Conrad. r
Pterygometopus callicephalus, Hall. cc

This variety is marked by acute, oblique wrinkles along the cardinal
line, such as occur in Strophomena rugosa var. subtenta,
andStrophomena incurvata @& S.filitexta). This feature
is constant in the vast numbers of valves which compose some of the peb-
‘bles in the conglomerate of Rysedorph hill (see p. 546) and Moor-
dener kill, and it continues upward into the Utica shale of Green Island,
and Menands, though in these localities forms with and without wrinkles
occur together. The same variety was observed by Dr Beecher in the
material from the Dudley observatory, and listed as Leptaena sub-
tenta? The wrinkling is apparently rare among specimens collected
‘west of the Hudson river region, for it is not mentioned in the very
-detailed accounts of the characters of this species in the west by Sardeson,
Winchell and Schuchert, but it was listed among the Cincinnati fossils by
Jamesas Leptae na as pera and has been figured by Hall and Whit-
field. (Geol. sur. Ohio. Paleontology. v.1. pl. 5. fig. 3 f.)

Climacograptus typicalis, Hall. 3: ona ee.
Corynoides curtus, Nicholson, roo ra.
Pholidops subtruncata, Hall. ro” 7
Dalmanella testudinaria, Dalman sp. cc
Plectorthis plicatella, Hall. c af
Plectambonites sericea, Sowerby sp. cc
Rafinesquina alternata, Emmons sp. ¢ | Ae ats
Murchisonia (Lophospira) uniangulata var. abbreviata, J
Lophospira bicincta, Hall sp. r
Archinacella patelliformis, Hall sp. c¢
Clionychia sp. n. rr. |

Cleidophorus planulatus, Hall. ce
Modiolopsis faba, Hall. ec

Cameroceras proteiforme, Hall. r
Triarthus becki, Green sp. r

Calymmene senaria, Conrad. r

Cyphaspis sp. rr

Trinucleus concentricus, Hall. ee
Ctenobolbina ciliata, Emmons sp. e

C. ciliata var. conuta var. n. ©
Lepidocoleus jamesi, Hall & Whitfield sp. r
A comparison of these two faunas from Green Island with that
discovered by Dr Beecher near the Dudley observatory at Albany
proves their identity. Dr Beecher considered this fauna as being

on stead Lorraine faunas of Block island

d 4 eae

2S er ina aiiatl as pit about a hundred yards
Menands station. The fossils are:
ag a eg te Dalmam sp. ce

| ¥ aiinites 5 ee pee sp. ce
ay P. sericea var. aspera, James var. ¢
Rafinesquina deltoidea, Conrad sp. rr
_ ‘Archinacella patelliformis, Hall. c
Bellerophon bilobatus, Hall. r
_Spyroceras bilineatum, Hall. r
Ctenobolbina ciliata, Hmmons sp. r
; The presence of Plectorthis plicatella and Spy-
roceras bilineatum_ connects this faunule with the
‘ faunas of Green Island.

Station 12. Devil’s Den, Watervliet

In a deep gorge, called Devil’s Den (station 12), behind Gen.
Schuyler’s historic home and half a mile west of Watervliet,
blackish and gray, fissile, soft argillaceous shales, somewhat
sandy toward the upper end of the gorge, are exposed for about
half a mile. These yielded a number of well preserved specimens
of Orthograptus quadrimucronatus, Hall sp.

1The association of Trenton and Lorraine forms in the same beds, and
the peculiar position of these beds in the Utica zone will be discussed
later (p. 564).

. 4 Soe
ye oy > at okie ae
ri mei! th feist
: BS JIUTICOLY
" ie yes \ * »
a > | y ) ae ee I
7 : m 7a -o*
FOP vat a, r
*
\ ‘ ’
Sp.
= :

in great p
fact in the best state of
ervation of rhabdosomes of graptolites ever seen by
writer in shale. Ghats Sat er.
Diplograptus putillus, Hall ra
D. spinulosus sp. n.
Corynoides curtus, Lapworth
Dendrograptus sp. ae
‘There occur in the shale of the Rural cemetery extremely fi 7
slender, chitinous, irregular branching threads of undoubted graptoli
nature. These are rolled up, the larger and smaller branches s sparat
into an intricate, irregularly convolute mass. Such a form has t
described and figured by Emmons American geology. 1875. pt 2 pid
pl.1. fig. 7) as Nemagrapsus capillaris. Hall did not re weet yc
nize the genus, as one of Emmons’s species, N. elegans, (sum
only a fragment of Coenograptus gracilis, and the rela-\is/r ag
tions of the other form, N., capillaris, on which neither thecae a
nor thecal apertures were observed, “can scarcely be determined from — >)
the figures given” (11:48; 13:211). The genus was later accepted by : er
Lapworth, but Roemer (54:587) remarks that Hall, having access to the , ‘aes
material, was certainly better prepared to judge its value. Ami (Bul. geol.
Soc. Amer. 1891. II. table p. 495) reports it doubtfully from the Can-
adian Calciferous; and Gurley, after having described a form as belonging
to Nemagraptus which he later recognized to bea Thamnograp-
tus, declares that he has found typical specimens of Nem agraptus
capillaris at Stockport, Columbia co., but does not describe them
(0:306), The writers material shows all the features indicated by
Emmons’s figure. Both the figure mentioned and the material suggest that
the fossils consist of the broken terminal fillform branches of some delicate
ramose graptolite which, drifting about, were rolled up. A comparison
with specimens of Dendro graptus tenuiramosus, Walcott
(19:21. pl 1. fig. 4) from the Utiea shale shows that our form on the

* =F
SE Te

a

on different surfaces of closely adjoining layers; only the

eo D. spinulosus mingling with the others, as if they

aaa

Ee A assorted according to their weight while drifting about.

The other graptolites of the Utica shale occur for the most part

Separately in the shales of the Mohawk valley; this is specially

notable of Climacograptustypicalis, Cl. bicor-

nis andDiplograptus ruedemanni.

Station 15. Old Dudley observatory, Albany

3 miles S SW of the Rural cemetery exposure and just north
of Albany, on Patroon’s creek near the old Dudley observatory
(station 15) is the exposure from where Dr Beecher, in 1889, ob-
tained the first unmistakable Utica fauna from the Hudson river
shales (see p. 502).

whole is more slender and flexible (only .1 mm wide), but its thickest basal
parts correspond in thickness to the terminal parts of that extremely

- delicate graptolite whose thin filiform ends also show at times an inclina-

tion to become convolute. Furthermore most of the branches possess the
same smooth, unindented character and apparently, though not distinct
enough to permit positive assertion, small pits along the median line. In
the absence of more complete material, it seems therefore justifiable to
consider this fossil as consisting of the broken, thin filiform ends of
Dendrograptus tenuiramosus or a Similar species.

18ee description of these fossils p. 574.

graptus putillus "a pete eo:

_ D. spinulosus sp. n. pay = = i$ er: a
Climacograptus typicalis, Hal
Leptobolus insignis, Hall ty) a
Undetermined brachiopod a
The first is the most common graptolite; it entirely s0ve on

slabs. a

Station 17. Beaver park = 3 a a

J. Van Deloo collected, some years ago, at the tim
laying out of Beaver park, a few graptolites in a rayin
northern part of the park. These on investigation prov re a to
specimens of Diplograptus putillus, Hall, indica fj
the Utica age of the beds of this locality, which is only a on 3 c ia
distance east of the preceding locality. “0 he ca

Station 18. Normansville

2 miles farther southwest, along the general strike of the rocks, — aa
is Normansville on the Normans kill. While at Normansyille __
itself, in the sandstones and shales exposed above and below the
bridge, no fossils were found, and the age of these rocks remains
in doubt, a small outcrop of shale about a mile farther up, 100
yards below the landing of the picnic ground on the right bank :
of the river, furnishes graptolites (station 18). The rock is a
deep bluish black, thick bedded argillite with conchoidal fracture —
and iron-stained cleavage planes. It is filled with specimens of

Climacograptus bicornis, Hall

Ses A Me”
7 ke

nD involved 4 in the bapereae of the Hudson river beds.

Station 20. Black creek, Widrhccaetite
_ Following the Normans kill no outcrops are found in its widen-

. "* ing valley or along any of the tributaries till reaching Black
___ereek, a small southerly affluent, 4 miles farther up (station 20).

The banks and the bed of this creek are formed of dark, often
black, soft, non-metamorphic, mostly argillaceous shales, from
which the creek derives its name. While near its mouth the
shale is slightly disturbed by a fault which, according to its south-
west strike, still belongs, as an accessory fault, to the Hudson
river system of faults, the shales farther up the creek show a
regular n 70° Ww dip and n 160° w strike, and lie hence outside
_ the easterly tilted block of the Hudson river region. The large
fault reported by Emmons and Ford as extending from Saratoga
Springs across the Mohawk river and separating the tilted and
folded Hudson river region from the undisturbed region to the
west, probably passes the Normans kill between the last two sta-
tions and may also account for the lack of outcrops and the
broadening of the valley between them. These black shales con-
tain:
- Orthograptus quadrimucronatus, Hall sp.
Diplograptus putillus, Hall
Climacograptus typicalis, Hall

=

ward, argillaceous shales, sas shales and aryeet ice
passed in manifold alternations. They show a general w ter
dip (20°), and in two places are thrown into a series ee ma
parallel folds, a few feet wide, striking n 15° e. These as vell
as a fault, which runs in the same direction, are evidently th
faint westerly outrunners of the powerful Appalachian ¢ stur
ances of the Taconic mountains and of the Hudson RES
region with which they run parallel.
Farther down, about halfway between the sawmill sat
mouth of the creek, black shales begin to replace the san nd -
stones and lighter colored shales. In one of the lower drab
beds of sandstone numerous large specimens of Clima- sais i
cograptus typicalis were found, indicating the Utica — tae
age of these lower sand beds (station 21). This*sandstone effer- _
vesces with HCl and is, hence, calcareous, like the Utica shale
of the Mohawk valley. In the dark gray sandy shales below
this sandstone, which, however, do not effervesce, were found:
Climacograptus typicalis, Hall
Sagenella ambigua, Walcott "ey
Cameroceras proteiforme, Hall sp. ia
It thus appears that along the Vly a section is exposed from :
the Utica shale into the overlying Lorraine beds. This outcrop
of Utica shale is the most southern and western which could be
found in the region studied, as this shale toward the Helderberg
mountains dips under the Lorraine beds, which in their turn

a "

em Ty “ta ae a

der] > ae the latter in the undisturbed region to the west of the
eae ep arating fault. Toward the north the zone probably connects
ae wie the Utica shale known from the neighborhood of Mechancis-
ville, Saratoga Springs, Sandyhill, etc.

C MIDDLE TRENTON BEDS
Station 22. Watervliet arsenal

The next group of stations (stations 22-26) comprises five locali-
ties which may be arranged in two rows extending from n ne to
S sw on both sides of the Hudson river south of Watervliet and
Troy. These localities furnish Trenton fossils. The occurrence
of the latter was first made known by Whitfield (see p. 496), who
reported the finding of Diplograptus amplexicaulis

at the Watervliet arsenal (station 22), and south of Troy in shaly

partings between layers of metamorphic limestone. The locality
at the arsenal is no more accessible, but part of the material
collected at that time is preserved in the state museum. It con-
sists of very soft bluish black, argillaceous shale, which does not
effervesce with HCl and is thickly packed with a long, narrow
graptolite which in dimensions, arrangement and form of thecae

Dalngarens testudinaria, "Emmons 5p

Plectorthis plicatella, Hall
Platystrophia biforata, Schlotheim sp.
Plectambonites sericea, Sowerby sp.
Rafinesquina alternata, Conrad sp.

*‘Diplogaptus cmb lexicailis wa) ito eae
the middle Trenton of Trenton Falls and Middleville. There, a |
at Trenton, it occurs in great profusion in certain beds of th the
Trenton, while in the Rathbone brook section, south of Trer = F
was also observed in beds considered as lower Trenton by L
White (51:86). Whitfield, as observed (p. 496) found it at the Vi Vater’
arsenal and at south Troy, and based on it his correlation aa th
shales with the Trenton. Gurley, who considers it as only an nutat
of D. foliaceus, assigns it to the Chazy (Mystic, an.) ar
Trenton. Joseph F. James records its collection in the typical
locality (Amer. geol. 4:237); Walcott mentions its being found in the
part of the Lorraine section (36a:339); and Whitfield enumerate
his catalogue (61:20-21) as D. amplexicaulis a number of .
types of Gr. pristis of Pal. N. Y., v. 1, from Turin, Lorraine, Collins
ville and the Oxtungo creek. It becomes apparent from these citations
that this graptolite is of rather uncertain value as an index fossil of the
Trenton; it has been reported from beds ranging from the Chazy to the
Lorraine, and probably the form is not yet well understood or D. foli-
aceus, to which it is closely related, has been mistaken for it. The
amplexicaulity of the thecae is not restricted to this species, the concayo-
convex section of the rhabdosome is not observable in flattened specimens,
so that in the determination of specimens from the shale one is restricted :
to the observation of the dimensions, outlihe of thecae and rhabdosome, |
and of the general habit. These characters, however, being subject to .
alteration by variations in pressure, are often difficult of exact observation. 1
The relations of this form to D. foliaceus and its vertical range
apparently need farther study. The writer has not seen typical speci-
mens of this form from beds of younger than middle Trenton age.

7 eS 1 ee ee

ae sig i ar ric S
Ou eyete

estas
a MeAneAE®

F i, “The outcrop south of Troy where Whitfield 26 years ago col-
: Be cied the Trenton graptolite, could not be precisely located; at
_ Jeast no information of the former occurrence of limestone in that
neighborhood could be obtained. There were, however, several

localities found which furnished ample evidence of the presence
of Trenton fossils and which, as they contain calcareous sand-
stone banks with intercalated impure limestone banks and shales,
may be identical with Mr Whitfield’s collecting ground.

The most important locality is the Brothers’s or Lavery’s quarry
station 24), at the brow of the hills east of south Troy. Diplo-
graptus amplexicaulis is found here in great numbers
in black, argillaceous shale at the east side of the quarry and
more sparingly in association with Corynoides calicu-
laris in similar beds at the opposite side of the quarry.

In calcareous sandstone beds which contain dark impure lime-
stone banks consisting of brachiopod shells, in the middle part
of the quarry, occur brachiopods, a number of which were first
collected by Gilbert Van Ingen of Columbia university and kindly
left with the writer; and one bed is filled with bryozoans. The
beds yielded:

| Rhynchotrema Increbesce ns Hal 7” = inaequivah
nau sp) 2S Pe eee Re
Proétus parviusculus, Hall ea
Of these species Schizocrinus nodosus “ind
Trenton age in general, while Pachydictya_ acut
ported by Hall (7: 75) as “of frequent occurrence in k
lower and central portions of the Trenton limestone”, a m
ment with which Winchell and Ulrich concur in 1 repor t sin,
fossil from the Clitambonites, Fusispira and Nematoj pora be
Minnesota (49: 111). Escharopora is, ance o
same authors, restricted to the Stones river, Black river, a
and central Trenton beds. Rhynchotrema increbé
cens, in the restricted meaning (i. e. with the exclusion of tl
distinct Lorraine form, R. c a pax, originally included by Hall in — ee
this species) is a Trenton form. In the west it occurs in the upt % ye eh ;
Black river group, lower and middle Trenton (49: exy) and i ate a
Canada it is found in Black river and lower Trenton. It is, — 3 .
hence, indicative of the lower or middle Trenton age of the Troy fee .
beds. Proétus parviusculus was originally described
by Hall (14: 223) as occurring “in shales of the Hudson river
group, Cincinnati, Ohio”. The correlation of these shales has,
however, changed since that time; for Winchell and Ulrich
cite the form from the Trenton of the Cincinnati region. Dr
Clarke (49: 754) reports it from the base of the Galena shales
at St Paul (Clitambonites bed, Winchell and Ulrich, which is
lower Trenton). In Canada it has also been found in the Trenton.

t : —- 4
a le Bs Pit eh) vie Ae ae

me
4 P.

e igecnogiee ae uiaten: ae in all ee aeaialsek
ecur gray, sandy argillaceous rocks with iron-stained fos-

ilarity is only accidental. i

Station 25. Ruscher’s quarry, south Troy
E ianétly south of the Brothers’s quarry and in the strike of its

: ee lies another large quarry, Ruscher’s (station 25). The same
black shales, heavy sandstone banks and arenaceous limestone

beds, as well as greenish shales toward the eastern part, are here
exposed. Diplograptus amplexicaulis is also quite

common. A

Station 26. Corner of Adams and 10th streets, Troy

In the railroad cut at the corner of Adams and 10th streets in
North Troy, (station 26) in a compact, black argillaceous shale
Diplograptus amplexicaulis, Hall, and Cory-
noides curtus, Nicholson, were found. These fossils and
the appearance of the rock leave no doubt of the identity of these
beds with those exposed in their direct strike in the Brothers’s
and Ruscher’s quarries in south Troy. No other exposures of
these beds have been met with farther north, in the investigated

area, though they undoubtedly continue in the direction indicated

by the outcrops in Troy.

rt

ce i id reginefrage eh vd in a

Trenton beds brings ise Wee ie mination of t
show, into the alluvial plain of the Hudson eet

are absent. The zone would then probably rent nro ag
lower part of the city of Albany and could be expecte ed al se
Normans kill above Kenwood and below the Utica s
crops described above. But along that part of the 1
one exposure is found, that at Normansville, and this
nately, is not known to have ever yielded any fossils. I From]
to the Lorraine sandstones and shales at the base of ne He
berg escarpment no farther outcrops could be found. 1
Viaumans and the Coeymans kills, which have been - 1
by the writer along their entire courses, show outcrops on eae
their mouths, and these belong to the next following zone.
outcrops at the upper Coeymans kill and its trib aie ei bY in
the Sprayt kill, have been mentioned above. On account of the

general n ne-s sw strike of all the beds in this region, it can, —
however, be safely surmised that this zone passes under the Hel- ec
derbergs. Ye

Be i
Pe

a Bes

i:

D NORMANSKILL BEDS (LOWER DICELLOGRAPTUS ZONE)

After the presence of these zones of Lorraine, Utica and Tren-
ton shales in the Hudson river valley had become evident to the
writer, a thorough search for the graptolites of the Normans kill
or lower Dicellograptus zone was instituted, this zone being, in
accordance with the views of previous writers, sought for be-
tween the Lorraine and Utica, and between the Utica and Tren-
ton zones. There has, however, no trace of these graptolites
been found between or within the Utica and Lorraine ZONES,

ah ae gray oe shales, farther down
mewhat sandy shales, and at the bottom softer, black
,ous shales are exposed. The last contain graptolites in
te of preservation; besides Corynoi des calicu-
; and a narrow Diplograptus which closely ap-
) 1es D. amplexicaulis; well developed specimens of
pl ograptus foliaceus occur in fair number. The

Station 28. Poesten kill, South Troy

The Trenton shales of the Brothers’s quarry appear again across
the Poesten kill in Spring avenue in a small road metal pit be-
hind the northern row of houses. Going from here 200 yards
Ee. east, along the north bank of the Poesten kill, just above Ruff’s
canal mills, a four foot sandstone bed is met with to the left
Fr of the road, which is overlain by black, strongly carbonaceous,
: argillaceous, rather thick bedded shales. These were found to
contain graptolites in considerable number and in a fair state
of preservation (station 19). There were observed:
Leptograptus subtenuis, Hall sp.
Dicellograptus intortus, Gurley
a D. sextans, Hall sp.
Climacograptus bicornis, Hall

ee ee ee
* ine =<. Re

C. parvus, Hall
Diplograptus foliaceus, Wwrehison sp.

Dicellograptus beds, and this interesting d is
the presence of the Normans kill fauna in a few hund ire¢ £
to the east of the middle Trenton fauna. e =
Following the section farther up along the Poesten k
nations of sandstones and black argillaceous shales are
with, then a four foot conglomerate with black shale :
at the water tower of the wire mill; above this ; ernatiol
fissile, black and greenish gray shales and finally, ye ei,
disappearance of the black shales, only green shales. On tl
other side of the Poesten kill, just below the Sicha
falls, specimens of Rhombodictyon were found in a b : <n
shale, intercalated in a green shale, the latter containing g
quantities of fragments of algae. These shales extend eastwar oe
as far as the great fault which brought up the Cambrian belie
against the “ Hudson river shales ”. ee

a a>.
“Som
Pile:

Z was

Station 29. Mount Olympus, Troy

Another outcrop of graptolite shale was found 2 miles farther
north at Mt Olympus, a landmark of North Troy, consisting of a
cliff rising some 60 feet above the alluvial plain. ce 4

The deep black, fissile argillaceous shales contain:

Didymograptus tenuis, Hall sp. rr >

Dicranograptus ramosus, Hall. r

Climacograptus bicornis, Hall. ce

Bead The black hale Pipnicahed:
calicularis, Nicholson. In immense number.

4
4
4

! ptus serratulus, Hall. rr
ograptus ramosus, Hall. r- ate
ograptus angustifolius, Hall. Completely covering some

cs aff. putillus, Hall. rr

: oe ‘D. foliaceus, urchison. sp.
DD. whitfieldi, Hall. c¢

Climacograptus bicornis, Hall. c¢

C. scharenbergi, Lapworth. c .

aS. 4. CC
cr Sp. 2. 6 | i

The faunas of Lansingburg and Mt Olympus, which lie in the
same strike and evidently belong together, differ in general as-
pect from that of the lower Dicellograptus fauna by the scarcity
of branching forms and the strong prevalence, in species and
individuals, of the biserrate graptolites, notably of the genera
Pipieorcraptus and Climacograptus. They ap-
proach in this regard the fauna of the upper Dicellograptus
beds, to which they could be referred, were it not for the occur-
rence of a few stipes of Didymograptus tenuis,

*The new species of graptolites will be described in a separate, later
paper.

be taken to suggest that we Wave! There dias arate
these beds do not represent another zone, but. ae a
upper Dicellograptus zone, the Diplograptus enplexi se 1

would seem partly to overlie with its beds at
and partly to be intercalated into, the lower Dice
zone, at station 27, east of Mt Olympus, an uiveatae
may be also caused by the complicated folding of © nee
which partakes of the nature of an anticlinorium (see ie
The entire problem, however, of the relation of these b
Lansingburg to the lower Dicellograptus and ‘Diplograptus
plexicaulis zones awaits its solution in the tracing of thea it re
system farther north at some future time.

Station 31. Bluff above Lansingburg Row “s ae

Directly opposite Laveny’s point, station 6, in a high bluff, nie 4 a
a mile above the Lansingburg-Waterford bridge, a fossiliferous x Aes
bed was found. The soft, fissile, black shale contained: Ta

Corynoides calicularis, Nicholson. r | 8

Diplograptus sp. Small fragment 4

Climacograptus bicornis, Hall. e¢

Climacograptus sp. n. ¢

These beds probably belong to the horizon represented by the
Lansingburg fauna. !

Following these sandstones, black gray and greenish shales
of the Poesten kill southward, a good section is met along a ereek
entering the river opposite Lagoon island. Here similar rocks
are exposed, which, however, did not yield any fossils.

am
ey
a

t-te poe egy ieee ae as s belonging Ht the legen
cies zone.

ape (station 33). eee exposed in a railroad cut and at

A : the falls of the Normans kill consist of thick, partly coarse sand-
stone banks with intercalated, glazed, grayish argillaceous

shales and some black shale from which the graptolites were ob-
tained (described in Pal. N. Y., v. 1 and 3).

Station 34. Glenmont (the Abbey)

Another locality which furnished fine material and still con-
tains graptolites is the cut.on the West Shore railroad, half a
mile below the station of Glenmont (the Abbey, station 34), where
similar beds with a thin black band, full of characteristic and

finely preserved Normans kill graptolites, have been exposed.

Southward from here, localities with this fauna have been found
on both sides of the Hudson river; on the west side as far as 70
miles south of Albany (27).

Station 35. Moordener kill, Castleton

There is first the fine exposure of ‘“‘ Hudson river shales” and
of the overthrust Cambrian beds along the Moordener kill or Mur-
der creek extending from Castleton on the Hudson, 7 miles south
of Rensselaer, to East Schodack (station 35). The section begins
opposite the mill of the Fort Orange paper co. with much con-

‘S

boyT i '
). a r ; ¢ .
ae TOOE a 2 ore Oh a Soh a Let ;
‘ le ae EUS Pane ie AP ae aon Pos
Corvr 1es calicularis. Niche 7) a
im — iy Uit . £iCU LLiS, 7

¢ oe > ae Mee yaa ae 1) hy i raetr fe pee, es
_The presence of Climacograptus parvus,
graptus angustifolius and I asiograpt

¢ronatus places this fauna in the lower

Dicellograpt
CONGLOMERATE BED OF LOWER TRENTON ASPE(

SHALE celts
- a

About 150 yards farther up in the nucleus of a tic
a conglomerate bed with black shales above and beloy yi
posed. The exact thickness of the latter could not, o ac
of the intricate contortions and the resulting swe ling uy a
thinning out of the bed within a short space, be made out in I
place, but the same conglomerate bed, or a very simila r one, |
farther up the creek proved to be about 13 feet thick and was
also inclosed on both sides by black shales. The matrix con- _
sists of a dark arenaceous limestone which weathers into a ¢ rab: ieace

sandstone, while the boulders, which are all well worn, consist =

i

,
~~

ro ~ on
of small pebbles of reddish or yellowish sandstone, probably of “ane

Potsdam and Beekmantown (Calciferous) age, of large boulders

(up to 1 foot in diameter) of light blue, hard Lowville (Birdseye) ee.
limestone with birdseyes and Tetradium cellulo sum, sam
Hall sp. (a typical Lowville limestone fossil), and of still larger
boulders (one 2} feet in diameter) of dark gray Trenton lime-
stone. The latter contained:

Streptelasma corniculum, Hall

Callopora cf. ampla, Ulrich. ¢

Plectambonites sericea, Sowerby sp. var. aspera, James. ce
Strophomena incuryata, Shepard sp. (=Str. filitexta, Hall) e¢
Rhyuchotrema increbescens, Hall. r

= 8s 26 bi ee ee ee

cc

Tus Be asi hart, H al. :
D alaria trentonensis, Hall. Young specimen. r
_ The matrix contained:

-Pachydictya sp. ¢

_ Stromatocerium sp. ce

- Rafinesquina alternata, Emmons sp. c

Plectambonites sericea, Sowerby sp. var. aspera, James. r
Strophomena incurvata, Shepard sp. r

Plectambonites, sp. n. aff. gibbosa, Winchell & Schuchert. r
Of these forms Streptelasma corniculum occurs,
according to Hall, principally in the lower Trenton; Winchell
and Schuchert report it from the lower and middle Trenton;
Callopora ampla and multitabulata are both Black
river and lower Trenton forms in the west; Pachydictya is
principally developed in the lower and middle Trenton; Stro-
phomena incurvata occurs according to Hall in the lower
Trenton at Middleville, is reported by White from the same bed
with Diplograptus amplexicaulis, and may there-
fore, rise into the middle Trenton; and in the west it is princi-

‘The new fossils of this and the next station will be described in a
separate paper.

eastern region, oniee that of the Pooks h
components and finally, its: intercalation in ‘the Nor ans
shales. ‘

CONGLOMERATE BED ON RYSEDORPH H ;

This interest is hightened by the occurrence of anot t]
glomerate bed on the top of Rysedorph hill or the Pir j
of Rensselaer (station 36 on map), which contains the sam ne
of Trenton pebbles bearing the same faunas, augmented, h Wey
by numerous other species, in part new. The pedulieas ) th
character of this Trenton fauna of Rysedorph hill finds its m
pregnant expression in the numerous specimens of Any be
hastatus sp. n. (see pl. 1, fig. 1) and Remopleurides $4 meee
linguatus sp. n. found in the game pebbles with ae
CeraurusandPterygometopus. As before ob-
served, Ami found similar antique forms in the Dicellograptus | a s1
zone of the Quebec massive. The different composition of this _
eastern Trenton fauna when compared with the other Trenton
faunas of the state, is a fitting corollary to the restriction of the
Normans kill fauna, with which it is homotaxial, to the eastern
margin of the state. Both faunas, together with Ami’s inter-
esting discoveries, point to conditions and connections of this

eastern border sea altogether different from those of the regions
to the west.

This is the locality termed by Emmons (Am. geol. pt 2, p. 72) and
Waleott “ Cantonment bill.”

-phogy arene aff. peerittes a a
ra (see pl. 1, fig. 1). The graptolite is a Clima-
A careful pee of it with all the spe-

ay . specially by the characteristic deep, Beis zigzag groove
; # along the median line of the rhabdosome. This is a character-
istic feature of Climacograptus scharenbergi Lap-
worth, with which it also agrees in the rectangular outline of
the thecae and apparent absence of appendages. Ol. scharen-
bergi has been reported before by Lapworth and Gurley from
_the lower and upper Dicellograptus zones (the former—Normans
kill zone) of Canada. It does not rise into the Utica and Lor-
raine beds. Its association at Rysedorph hill with a peculiar
lower Trenton, fauna, is, hence, a strong argument in favor of

the lower Trenton age of the Normans kill shale.
In Europe this graptolite occurs at even deeper horizons; for
Roemer (54:612) collected it in the Phyllograptus shales near
Christiania, and Tullberg reports it from the horizons with

a

Didymograptus geminus and Diplograptus
putillus, which, in Scania, lie below the Coenograptus
gracilis zone (—lower Dicellograptus zone). In Scotland it oc-
curs in the corresponding Glenkiln shales, which also lie deeper
than the zone with Coenograptus gracilis which forms
the base of the Moffat beds.

The beds on Rysedorph hill which outcrop at the fault be-
tween the Normans kill shales and the Cambrian slates repre-

This wiald i in ‘ peat
Pt at earns meh ye ener ki : Be 7
that it is, like the wee nelosed in the shales, and
continuous with it. A few lie south ‘of Cs stleton ai
brecciated limestone bed, intercalated in graptolite-be paring
mans kill shales, was discovered by Ford (see p. 503). This |
directly in the strike of the Moordener kill bed po is or 0 robal }
also continuous with it. tn ag
The conclusion to be derived from the observations ee e
conglomerate beds, which is of the greatest import for the pi
ent investigation, is that there is intercalated in undoubted N
mans kill or lower Dicellograptus shales a conglomerate
which, in pebbles as well as matrix, contains as its youn i ee
fossils those of lower Trenton aspect. The occurrence of . as
bles of two different kinds of limestone (even three at yi ie a
dorph hill) means that the formation of several Trenton — ‘Loe
limestone beds must have preceded the deposition of these i |
shales, and that an unconformity exists between the lime- s 2
stone and the shale. The more common fossils of the
pebbles have however been found also in the matrix. This
could be explained either by the assumption that some fossils Me
became separated from the pebbles and embedded in the
matrix, a view which seems to be supported by the scarcity of
fossils in the matrix and opposed by the occurrence of whole
specimens of such fragile shells as Strophomena in-
curvataandPlectambonites sericea var. aspera,
James; or by the assumption that the forms entombed in the
pebbles were still flourishing at the time of the formation of
the conglomerate. As the conditions of living in a region where

i a Pe

i DN Tee idee

HUDSON RIVER BEDS NEAR ALBANY 549

the deposition of large boulders proceeds are evidently not favor-
able to a benthonic fauna, the scarcity of fossils in the matrix
appears natural; and the view of the continued exisience of the
fauna of the pebbles, in some adjacent region, and its occasional
incursion into the graptolite province seems to be the better sup-
ported. This would mean that the Normans kill graptolite fauna
and the mollusk and trilobite fauna of the conglomerate with
lower Trenton aspect were synchronous. The presence of Tren-
~ ton fossils in so-called’ Hudson river shales has been proved be-
fore (see p. 536). So has the resting of these shales immediately

on lower Trenton limestone beds in the regions to the east (83)
and to the south, near Poughkeepsie (21).

Following up the Moordener kill to the base of the second.
falls, black shales with intercalations of hard, black chert beds
and some thinner, sandstone and limestone bands are passed,
and at this point a conglomerate bed, 18 feet thick and flanked
by thinner conglomerate beds, crosses the creek. On account of
the disturbed character of the region, this bed may be identical
with that first mentioned. The shales continue tothe third
falls, where a third conglomerate bed, 20 feet thick, is met with.
Then follow coarse sandstones in layers from 2 to 4 feet thick,
and sandy shales, and above them black, fissile, argillaceous
shales with many thin intercalations of dark limestone and sand-
stone. After a break of some 300 feet, dark gray, fissile shales
again appear, and these continue to the bridge over the Moor-
dener kill on the road between Castleton and Schodack depot
(Brookview). Just below this bridge, in steel gray, somewhat
sandy, argillaceous shales, numerous excellently preserved speci-
mens of Corynoides calicularis were found. This
occurrence suggests that all these beds may belong to the Dicello-
graptus zone.

A mile and a half farther up, the creek passes again over
olazed gray and black shales and bluish quartzite beds, followed,
below Dickerman’s mill, 2 miles below Schodack Center, by the
green and purple slates and grits of the Cambric formation.

black, crapiolit-bearihg aaah 8a arry at the nort
Mt Moreno where the alternating bands often do ie. - e
inch in thickness. “A Bi.
The presence of the Normans kill fauna at the Poe este
Troy, at Rensselaer, the Moordener kill, Schodack Ls :
Kinderhook creek and Hudson, all east of the Hudson r
at the Normans kill (Kenwood) and the Abbty (Glenmon
of the river, demonstrates the presence of a zone of } Norman:
kill or Dicellograptus beds to the east of the other lo :
glance at the map will show. This zone may =< W
through Vermont into Canada. It has also been found in Maiz
(39).

- 53 eee
TAXONOMIC POSITION OF THE NORMANS KILL GR : APS 4

TOLITE BEDS ’ i @
In the region northeast, east and southeast of Albaanea I

Normans kill zone is cut off by the overthrust fault which
brought it in contact with the Cambric beds. Farther south it et
has been found to rest on lower Trenton limestone (33). These — i .
Trenton limestone beds, which are in the north only indicated by _
the conglomerate beds of Rysedorph hill, the Moordener kill and
Schodack Landing, would, hence, constitute a fifth zone. Be-
tween this zone and the zone of middle Trenton shales and lime-
stones, outcropping at Watervliet and south Troy, is now inter-
posed the Dicellograptus zone. There can, hence, in the mass of
“Hudson river shales” be discerned four zones from west to east,
namely:

r
|
.

one ; There is first the aie between the typical lower Dicello-
_ graptus beds and the Dicellograptus beds of Mt Olympus and

4 Me Lansingburg; farther the remarkable admixture of Trenton fos-

sils and the presence of the Climacograptus caudatus,
which is a typical upper Dicellograptus form, in the Utica beds
of Mechanicsville, and the appearance of Cryptograptus
tricornis among the Utica fossils of Van Schaick island.
These latter faunas differ markedly from the typical Utica grap-
tolite fauna of the Rural cemetery, the penitentiary and the lower
Normans kill. There is finally the peculiar combination of Tren-
ton and Lorraine forms with the Utica fauna of the old observa-
tory and Green Island. 7

The full list of the various faunas observed is the following:

Lower Trenton fauna of conglomerate beds of Rysedorph hill,
consisting at least of three different faunules

Typical lower Dicellograptus fauna
Lower Dicell. fauna of Mt Olym- { Relative position of
pus and Lansingburg { these two faunas not
(| Dipl. amplexicaulis fauna | yet clearly determined

Trenton

of the larger divisions as not been etitieeee nus { ars
expected that a continuation of this: vestigation x th :

adjoining north and south will furnish the desired in fort m

EXPLANATION OF THE OVERTURN OF THE STR.

All these beds now dip east and the Lorraine beds a
the lowest in the series (see fig. 5, p. 556). It is, the for
sary to assume either a series of parallel overthrt st
brought up deeper beds successively or a complete overt
the whole series of strata. The former assumption wo ni ee
to find some support in the abundance of slickensides and s1
faults in some localities, as specially in the Brothers’s quarr
south Troy and along Dry creek, west of Watervliet. Bui it
could hardly be supposed that a system of larger faults could” ; ;
produce such a regular succession of zones following the genera * ane
strike of the beds as that found in the investigated area, without 2 ea
repetition of zones or other irregularities. The slickensides,
which are often not a foot apart, might be assumed to indicate
an upward movement of the entire mass along an infinite number
of small faults, such that the more easterly beds were regularly
pushed a little farther up, in a manner illustrated by Van Hise
(58) to show the possible great surficial elongation of the crust
by small displacements along shearing joints. Under such as-
sumption the whole orogenic movement would evidently have
been uniform and would have, regularly and gradually, brought

‘ a + ae as ¥
| a. =a) : ie °

a involving a ik disturbance of the aes succession.
a eit does away with those elements of uncertainty as to the un-
- broken succession of the four zones which would be involved in
the assumption of inversion by an overthrust system. Argu-

ments in support of this view are therefore here presented.
It is an established fact that the numerous folds of the Ap-

, palachian mountain system have their steepest slopes facing the

northwest or the interior of the continent and are more or less
overturned in that direction. The presence of the Appalachian
system of folds in the middle Hudson valley region was first sug-
gested by Mather (4) and asserted by Hall (15), who proved the
existence in the Catskills of four lines of very low anticlinals,
nearly parallel to each other and running from southwest 'to
northeast in conformity with the ordinary trend of the Appalach-
ian ranges; the synclinals occupying the summits, the anticlinals
the bottom of the valleys. This discovery has been verified by

Arnold Guyot (25).

. Two years. later the existence of folds of true Appalachian type
in the region between the Catskill mountains and the Hudson
river was reported by N.S. Shaler (18). On the other side of the
river it was found by James D. Dana that the schists of Hudson
river age dip under the limestone of Trenton-Calciferous age in
the limestone belts of Dutchess county and western Connecticut.

range to the pW tke, ‘errito}
type has been demonstrated by I. 45) in
paper in which it is shown that the Hiosars a3 puntair
cline. “This anticline preserves the rocks in their 1 | 7"
tion on the east side, but on the west they are folded v
inverse position with eastern dip.” ;

With the presence of folds of Appalachian type to the | $0 1 ‘h
and east of our region, the assumption of an ae t
underturned west sides to éxplain the inversion of the 2 1e8,
does not seem to be hazardous. Boe. ee

It was long ago proved by the Professors Rogers (2) that fe
great faults in southwestern Virginia lie in the direction of a: nie
of plications instead of in monoclinal strata and “coincide i in the ee =
great majority of instances with the steep or inverted sides of | a ;
the flexures.” It has been farther demonstrated that overfolds
often ¢hange into overthrusts, and theoretically should do so, as _
soon as the differential] stress of the layers reaches their ultimate
strength (see the lucid exposition of these relations by C. R. Van
Hise, 52). The wonderful regularity with which these ovyer-
thrust faults appear in the steep western sides of the numerous
folds of the Appalachian mountain system has been fully de-
monstrated by Bailey Willis (48).

‘One of the profiles has been copied to illustrate this type of mountain
structure. (See fig. 1)

°

Fig. 2 Overfolding of Appalachian type (see fig. 1) in Hudson valley of Albany. a=Cambric;
b=Beekmantown limestone (Calciferous); c=lower Trenton limestone; d=Normans kill shale ;
e=middle and upper Trenton shale; f=Utica shale; g=Lorraine beds.

2 The formation ofa fault in the underturned wing parallel to
the axial plane (fig. 3).

Cm cQomwr

Fig. 3 Fault in underturned wing of fold.

4 Reduction to a’plain. The erosion, working Dt '
to the elevation of the beds and, later, on the abrasi
seas of upper Siluric and Devonic time, as evinced by th
formable deposition’ of the limestones at Becraft m
(Columbia county), on the “Hudson river” shales, reduced
surface of the disturbed area to nearly or entirely the condi )
of a plain, leaving the steeply dipping conformable and in rel t
series of beds and the overthrust fault as witnesses of the orm ;
powerful activity of orogenic forces (fig. 5).

‘-
JIVO.
a ih

ISN SS SRST,
~~ NEAM ASN
SNe SASS
Stn SPONSE ce”

> ee
‘-~> :

Fig. 5 Profile through Hudson valley at Watervliet.

The small anticlines crossing the Vly are the weak western 4
manifestations of the fold-producing forces; for they run parallel .
to the greater deformations of the crust in the east, while the
larger anticlines, pretty examples of which are visible along the

ular. ly and nae anes pie sane
ticlinorium es si evnewed in this light these

me ‘the presence of such viding folds of various sizes to ex-
- ee ay eularities in Be srs of the beds cee

ern ay eastern Green isn, where we should expect the lowest
eae Utica beds. Also the apparent intercalation of shales with
Diplograpt us amplexicaulis in lower Dicellograptus
shales, east of Mt Olympus, may, on farther investigation, find its
explanation in such minor folds.

‘The end which the writer has in view in discussing the tectonic
relations of the investigated area is to demonstrate that the in- »
verted position of the beds can be brought into harmony with the
general structure of the whole region, and that this inversion,
therefore, can not in any way be construed as weakening the con-
clusion drawn from the succession of the zones and the paleon-
tologic evidence, viz that the Normans kill or Dicellograptus zone

1The possibility that the whole region investigated is built up of nothing
but closely packed, overturned small folds, such as were found by Shaler
farther south (18) and are described by Dale(63) from the slate belt, has not
been discussed by the writer, though the presence of such small folds can
be observed in several localities; for, on account of their small size and ev1-
dent surficial character, they would not be able to produce such long and
wide belts of rocks, as for instance that of the Utica shale. Dale
(63:199) also reports that in his territory, the northern extension of our
region, “‘series of such various folds form compound anticlines, and these
minor Cambrian anticlinoria alternate with Ordovician synclinoria con-
formably overlying Cambrian ones. As the Ordovician area consists of
shales, slates, grits and small quartzite beds, the beds being more hetero-
geneous, slaty cleavage is less prevalent, but the folds are also overturned
toward the west”’.

containing lend ‘Trenton ‘tomedle; — = over} 7
shale rests on lower Trenton limestone. yt

CLASTIC DEVELOPMENT OF TRENTON IN} 1UDSC
RIVER VALLEY ay

It seems appropriate to state here certain inferenc ne i
can be drawn from the principal conclusion of this paper
which seem either to militate against other well known f
the geology of New York or apparently are difficult of e:
tion. |

There is first the shaly development of the mass of the 1 rent 1 mt ty
in contrast to its typical caleareous character a short disté |
the west; for the correlation of the Normans kill shales w id
of the lower Trenton, of the Watervliet beds with the mid ldle ae
Trenton and the absence of limestone beds between this cat
the Utica shale zone necessitate the assumption of the replacing —
of the Trenton limestone principally by shales and sandstones. —
This view harmonizes with the well-known fact of the clastic es
development of the majority of the formations in the Appal-
achian region, to which the investigated territory, by the char-
acter of the disturbances and of those of the neighboring regions.
belongs. This clastic character and the great thickness of the -
mass of shales are both characteristic features of the Appalachian
region, and of themselves constitute evidence in support of the
structure indicated.

‘fs fia Sel
il i ud &

Walcott (36) that at Mt Anthony (Rensselaer county), where 400

; Re .
tg feet of limestone occur, Maclurea and Murchisonia are
found ‘nearly 200 feet below the shales”. The Trenton limestone

could, therefore, at that locality reach 200 feet at the utmost,

_ from which figure, however, are certainly to be subtracted the

measurements of the Black river, Lowville (Birdseye) and upper
Chazy limestones, which reduce this figure probably by one half.
In contrast to this stands the thickness of the Trenton limestone
in the typical section at Trenton Falls, where though the top
and bottom of the formation are covered, 270 feet were obtained
by Prosser and Cumings’s careful measurements (56). It is a
highly interesting fact that, according to the figures obtained
by the same investigators, the Trenton limestone gradually thins
out in approaching the Hudson valley region. At Littlefalls only
104 feet of limestone was found between the Lowville limestone
and the Utica shale; at Canajoharie and the Flat creek near
Sprakers only 17 feet of Trenton limestone; at Tribeshill, 40 feet;
along Morphy creek between Cranesville and Amsterdam, 37
feet; and opposite Cranesville, 21 feet; while Walcott reports
only 40 feet of Trenton limestone from Saratoga, north of the
region under consideration.

21 feet). In the well- aa at Altamont (37) 3475 fe es
between the Upper Siluric and Trenton limestone was f found ;
in Washington county the ‘thickness of the “ Hudson rive
shales” has been estimated by Walcott at 5000 feet (oes ah

This decrease of the Trenton limestone eastward of Trer
Falls and the increase of the superjacent shales are, howe y
to be understood as implying that the shaly facies of the 1 Tre
limestone, specially the Normans kill shale, gradually repl: cat Ss
calcareous facies, for the Utica shale has been found ey :
in the Mohawk valley to rest on the Trenton Vimastieel ag the?
Normans kill fauna is as yet unknown west of the Hudson river Bhi:
valley; but it certainly shows that either the conditions for the ae

<

formation of calcareous deposits throughout Trenton time became _ >» a
less favorable toward the east, and hence the calcareous forma- e se

‘The last estimates seem not to be verified by later observers. Dale (44) oe bs F
observed the dwindling in the thickness of the Hudson river shales in the
region east of the Hudson to “400-feet and possibly even 200 feet”, This
phenomenon is attributed to a replacement of the shales by grits or an
erosion of the former before the deposition of the latter. The same cause
is admitted as probably explaining his low estimates (1000 to 1200 feet)
for the Ordovician of the slate belt in his last paper (68:179). Kimball
(42) also found in Columbia county only 1285 feet of Hudson river shales,
but there also the series may have been reduced by subsequent erosion.

It is to be remembered that only the Normans kill graptolites have been

found thus far in the above mentioned Hudson river shales and slates;
and that, if this 1200 feet represents only the thickness of the Normaas
kill zone, which is still to be followed by the overlying formations, middle
and upper Trenton, Utica and Lorraine shales, this would bring the thick-

ness of the entire series nearer to the figure given by Ashburner.

he ps by a shalloasiie of ie sea as Ae rey phot Seen
on of limestone in the region of the lower Mohawk, in early
ant re nton time. The very peculiar Trenton fauna of the limestone
pcm \glomerate of Rysedorph hill and Moordener kill, characterized
pay the occurrence of Plectambonites sericea var.
. repern Plectambonites aff. gibbosa, Chris-
Be tiania, Eccyliopterus, Ampyx and Remopleu-
Be pei des, indicates a great faunistic difference between the Hud-
a — son ries and Mohawk valley regions even before the deposition
= of the Dicellograptus zone, and at the time of the deposition of
Y ~ the basal Trenton limestone beds.

DISCONTINUITY OF FAUNISTIC SUCCESSION IN TREN-
TON AND UTICA BEDS

A fact apparently incongruous with the separation of the Nor-
mans kill and the Utica shales by the middle and upper Trenton
4 beds is the discontinuity of the faunistic succession in these Tren-
_ ton beds; for, while the lower Dicellograptus fauna disappears
in the middle Trenton shales, a small part of the graptolite fauna
of the Dicellograptus zone reappears in the Utica shale. It is
this observation which induced Whitfield and Walcott to connect
the Normans kill with the Utica shale. On the other hand, the
graptolite, Diplograptus amplexicaulis, common
in the middle Trenton, disappears in the Utica shale and is said
to reappear in the Lorraine beds. The latter fact is in accordance
with the known return of other Trenton forms in Lorraine times.
The explanation of this alternating recession and return of grap-
tolite faunas in the Hudson valley region seems to lie in the dis-
tribution of the faunas and the character of the associate forms.

Gtx Fi Sepsis are
clea algatn pe

Trenton of the rest of New York nek Su st dire
west of it. Here is the genus Ch sintieutciee oat: i: |
been found in the Lower Siluric of North America, b D
that era in European waters, the Bohemians genus P stem
which is well represented in the Normans kill shales and ¥ |
besides has been found only in Canada and is therefore res be : a d
to the continental margin; the trilobite genera Agnost sy
Aeglina (rediviva Barr. ?), Ampyx, Dionide(? ob-
served by Ami with the Normans kill graptolites, and d the g enera
Ampyx and Remopleurides in the conglomerate b
Rysedorph hill, all forms which had apparently become extinct in
the typical Trenton of New York, but continued to live in Europ me |
Furthermore, as the Normans kill graptolite fauna has been |
found by Lapworth to be an exact correlate of a European grapto- —

Be: oa

lite zone, the conclusion seems to be unavoidable that the Nor- — as:
mans kill or Dicellograptus fauna was foreign to the American — ae
continental platform east of the Mississippi but was at home in 4
the oceanic basins of lower Trenton time and entered North pe
America along the eastern continental shelf. ‘aad

The middle Trenton shales of south Troy and Watervliet are,
by the oecurrence of Diplograptus amplexicaulis,
and Proétus parviusculus, connected with the Trenton
of Trenton Falls and the eastern Mississippi basin.

The Utica graptolite fauna is again fully represented in Europe,
and quite certainly entered the North American continent
from the northeast, as asserted by Matthew (47) and the writer
(50). Perhaps, as suggested by Frech (54. 2:100) the highroad

|
|
|

; still more emphasized toward) the interior of the continent
oi’ he overlying Richmond beds) is again evidently an epicontin-
ental fauna derived from the Trenton fauna. —
To state it more concisely, the writer believes that the Trenton
: fauna and its derivative, the Lorraine fauna, are of epicontinental
7 origin, and entered the Hudson valley region from the west, while
the Dicellograptus fauna and its derivative, the Utica fauna, are
foreign to the continent, and entered it from the Atlantic ocean
by way of the Canadian basin. This follows from the necessary
assumption of the presence of a Paleo-Appalachian continent
(see Frech, 54) to the east of North America. The former assump-
tion seems to be supported by the indications of the presence of a
ne—sw current in the Mohawk region during the Utica epoch,
found by the writer in the prevailing arrangement of the grap-
tolites, cephalopod shells, sponge spicules, etc. in the shales (55).
Lapworth, followed by Walther, maintains (53) that the grapto-
lites were planktonic or rather pseudo-planktonic animals which,
drifting along the coasts, left their remains in the quieter waters
at a certain distance from the coast. This view would also sug-
gest that the Trenton and Utica shales were formed along the
continental shelf under the influence of currents entering from
northeast. The alternations of coarse, mostly barren sandstones
with fine grained, muddy graptolite-bearing deposits indicate the
changing conditions along this coast shelf, which, on the whole,

‘i eS « Shy |

ead

*
a
= of

&
aue

river group”, or its ; on, “Hudson gi up’, ai
by Walcott for all the beds between the Trenton limes
the Upper Siluric. As the term has been so ably « nd 1
defended by such authorities as Hall (17) and Walcott (36a),
validity can be questioned only after obtaining new facts Ҥ

*A parallel case to the continued appearance of genera in—

Dicellograptus shales and the conglomerate of Rysedorph hill, whi
disappeared in homotaxial beds of other regions of eastern North . .m¢
is the continuation of Trenton forms which nowhere else have been «
served to go above the Trenton, as Parastrophia, hemiplicata,
Cyclospira bisuleata, Clionychia undata § PYTO.
ceras bilineatum, Cyrtoceras annulatum, Crypto
sraptus tricornis, and Climacograptus caudt cane
into beds which by the general character of their fossil contents are char- —
acterized as being of Utica age. This phenomenon has been observed in
several localities, at the Dudley observatory by Dr Beecher, in-
two outcrops on Green Island, one on Van Schaick island, and ¢ ne
south of Mechanicsville by the writer. The beds near Mechanicsville -.
may be here excluded as being evidently transitional between the n- a
ton and Utica epochs, or of oldest Utica age, but the other beds lie at or — -"
near the top of the Utica terrane and yet contain Trenton forms stil. B
This peculiarity in the composition of the Utica faunas is, to the writer's Bs
knowledge, restricted to the Hudson valley region, and therefore, marksa _ :
regional difference in the character of the Utica faunas. This conclusion
is supported by the distribution of Corynoides eurtus mentioned
before. This graptolite disappears in the Utica beds of the middle
Mohawk valley, while it fills the beds of the lower Mohawk and the
Hudson valley, and is also common in the Utica shale just above the Tren-
ton at the Panton shore of Lake Champlain. Also the variety of Plee-
tambonites sericea with wrinkled cardinal margin, mentioned
before, is a fossil which extends in this region from the lowest Trenton
into the upper Utica beds, and is rarely observed outside of it.

“

HUDSON RIVER BEDS NEAR ALBANY 565

the writer trusts, have been secured in sufficient quantity to
justify a reopening of the discussion.

Both investigators based their defense of the term on
the supposition that the entire series of the Hudson
river shales, though in diminished thickness, continued
into the Mohawk valley, and that these, like the Mohawk
valley shales, represented only the lapse of time _ be-
tween the Trenton and Medina formations. This supposition,
though at that time warranted by the facts at hand, has now
proved to be only partly correct; for only the Utica and Lorraine
shales of the Hudson valley continue westward, while the
apparently enormous mass of Trenton shales does not leave its
confines. The term could then be applied only to the shales in
the Hudson valley north of Cohoes and in the hills on the west
side of the valley as far south as Albany, while the shales all

These two differential features of the Utica faunas of the Hudson valley,
viz, the ascension of the Trenton forms and the restriction of the different
faunal composition to the marginal region, are evidently to be traced to the
Same cause. The assumption that these Trenton forms continued to live
in Utica time in the adjoining Atlantic basin, while they had become
extinct on the American continental platform, and thus were enabled to
leave their shells in the deposits of the eastern continental shelf, seems to
offer a reasonable explanation.

At the same time it is evident that in this region the change in physical
conditions from the Trenton to the Utica epoch was by no means so pro-
found as in the Mohawk valley and west of it; for there Utica mud shales
follow more or less pure Trenton limestones, and here the deposition of
clastic sediments was uninterrupted from the lower Trenton to the top of
the Lorraine. Such forms as in Trenton time were accustomed to live under
conditions that led to the deposition of mud and sand had of course a
much greater chance to continue living when the Utica time was ushered
in, in such easy stages as are apparent at Mechanicsville and on Green
Island, than the faunas farther west. But it is, then, pertinent to ask
why these forms did not wander with their new Utican companions, which
came across these marginal areas on the continental platform, into the
interior. This latter fact and the restriction of the graptolite, Coryn-
oides curtus, to the east suggest again that this regional difference
is of a character similar to that between the Hudson river Trenton and
the continental Trenton, viz, a difference between the oceanic fauna,
encroaching on the continental margin, and the fauna of a shallow con-
tinental and partially inclosed sea.

thereliee: that the term “Fludeon saftey r the bee:
tween the Trenton and Medina (Oneida) formations «
dropped. Clarke and Schuchert (62) have pies
“Cincinnatian”, for this interval in the geologic tines
North America. This term has the advantage of derive
a region where not only the Utica and Lorraine ©
fully developed, but where also a stage which intervenes b
the Lorraine and Upper Siluric age, and which is miss
York, viz the Richmond stage, is present. la
It would hardly be appropriate or practical to transfe1 - the
term, “Hudson river shales”, to the shales of the Normans k ill « -
Dicellograptus zone, which indeed is fully developed in the Had
son river valley and is seen there to rest on lower Trenton 1 ime 2
stone and to be overlaid by middle Trenton shales. As a tan
which faunistically and lithologically differs strongly from the
synchronous lower Trenton limestone, it certainly deserves to be ae .
designated by a separate name. Ami used the term, “Quebec one Ph
upper division of the Quebec group”, for the same facies, while ‘
Walcott, in the discussion following the reading of Ami’s paper,
suggested that the term, “Quebec”, be restricted to this upper
division alone in distinction from “Lévis” ete. In the Quebec
massive the beds are cut off from the neighboring terranes by
faults, and their taxonomic position can not be fixed conclusively
by the stratigraphy of the region, but the equivalent shales of the
Hudson river valley are well defined in their stratigraphic posi-

i
ae
i

tion.

Ss g a hil Be ey one in Genaon ie rinienite which
mee beds with Diplograptus pristis and D.
rimucronatus. It would seem more correct to

closer investigation of the vertical distribution of the graptolites
.and the possible more detailed division into graptolite zones of
ye the graptolite beds of the entire middle and upper Lower Siluric.
Meanwhile, and perhaps even then, the term, Normans kill shales,

may be of good service in designating this graptolite bearing,
clastic facies of the middle Lower Siluric.

SUMMARY

This paper purports to demonstrate the presence of four zones
of shales in the “Hudson river shales” of the Hudson valley
region about Albany. These zones, which extend from n ne to
S Sw consist, going from west to east, of shales containing the
Lorraine, Utica, middle Trenton and Normans kill graptolite

faunas. The shales last named include lower Trenton conglomer-

ate and rest on lower Trenton limestone. This succession of
zones places the Normans kill graptolite beds, which form the
mass of the “Hudson river shales” in the Hudson river valley, be-
tween the middle and lower Trenton and determines, together
with other facts, the lower Trenton age of these shales.

river shales”, for Gis upperendet pack Oe Lo is
the term, “Hudson river group”, for the Utica con Lorr a

and to employ the term Normans kill shales for the el
of a part of the lower Trenton which is charact
graptolite fauna at the Normans kill. __ + hitaeee

ome a usually 1 erected! as “ oholoid shells”, Bishop
several igo of means

have ee to be so well preserved hat they deserve mae
Pree different forms have been made out.

1 Paterula amii, Schuchert. Synopsis Amer. foss. Brach.,
bul. U.S. geol. sur. 87: 301

Paterula (?) sp., Hall and Clarke. Pal. N. Y. 1892. v. 8,
pt 1, pl. 4, fig. 1 (see pl. 1, fig. 2) 7

This is one of the more common forms in the shale. It is char-
acterized by its oval outline, broad marginal border, narrow,
marginal pedicle fissure, radiating muscular impressions, and its
rather strong, lustrous and well preserved shells.

The dimensions of the figured specimen were 3 mm (length)
and 2.5 mm (width).

As the specimens which were sent to Professors Hall na
Clarke by Mr Ami came from the beds of the city of Quebec,
which contain the same graptolite fauna as the shales of Mt
Moreno, it is very probable that the forms from the two localities
are identical.

2 Leptobolus walcotti sp. n. (see pl. 1, fig. 6-12)

The most common brachiopod is a larger shell of subcircular
outline, as usually preserved, very slightly convex and provided

position is strengthened by ‘the ovbalinenet of
shells, furnishing various transitions to thicker, sn or
foliated valves. The latter, instead of becoming ¢
yielded to the pressure by resin! ee in two or
ments (see fig. 12). wk

The presence of a strong median seutaue a por
traces of curving laterals and a posteriorly situated m &
cular scar in the brachial valve, as well as of a narrow p . .
groove below the beak of the pedicle-valve, indicate ea: ‘pos
in the genus Leptobolus.

It differs from all other species of Leptokalea w
larger size. Young valves closely resemble specimens of |
tobolus insignis, but differ in being less convex, havi
a less prominent beak, a thinner shell and specially a more reg
lar and finer concentric striation, af

Dimensions. The largest specimen observed attains a width
of 10.2 mm and a length (not fully preserved) of 8 mm. ak

Lower Trenton. Normans kill shales. Kenwood and Glen- |
mont, near Albany, Mt Moreno, near Hudson.

3s Schizotreta papilliformis sp. n. (see pl. 1, fig.
3-5)

em,
qe

we
las
A YS

A third very rare form among the brachiopods of the Normans
kill shales has been recognized as a new species of Schizo-
treta.

Diagnosis. Pedicle-valye subcircular, depressed conical, slop-
ing equally in all directions, beak abruptly projecting just behind

eviorly acral ib ak neti
eprese rres ponding brachial valve. | Ca
Length 1 of type | specimen, 3 mm, width 3.2 mm.
om | Sch. ovalis, Hall and Clarke, of

L
Pr A
Hr 1 =

: ant caries Serecinis siiation in common with Se a
ay pe aa: Pp ea, Billings sp., from the Canadian Trenton and Galena
i Bes. and Salmon river (Hudson river) formation of Minnesota
: (49: 365), and with the interesting Sch. minutula, Schuch-
ert and Winchell (p. 366). The latter occurs in abundance asso-
_ ciated with stems of Diplograptus in the “lower portion
of the Hudson river group near Granger Minnesota” (=Utica
shale). Sch. papilliformis differs from both these species
= in size, the more central position and more abrupt elevation of
the beak or apex, and in the presence of a distinct pedicle-groove
e, instead of the apical circular pedicle opening of the others.

It will be seen that these minute brachiopods do not directly
determine the position of the Normans kill graptolite shales, as
all three species are peculiar to this horizon, but their relation-
ship to Trenton and Utica forms of the genera Leptobolus
and Schizotreta, would certainly suggest the Trenton-
Utica age of the shales in question.

It is certainly peculiar that only these minute, thin-shelled,
non-calcareous brachiopod valves and no other fossils occur asso-
ciated with the graptolites. Their size, thinness and the com-
position of their shells indicate strongly that they led a pseudo-
planktonic life. Winchell and Schuchert suggest that Sch.

| ‘Technophors
19-25) n ae ante
Shell sive? eee convex, aka length : wit
hight, greatest length in about the middle, subalate- ost st
cardinal margin short and straight, anteriorly Lona
concave posteriorly; anterior end rounded, ventral r
convex, then gently concave, the postero-basal part
the posterior margin slightly concave, vertical; Be ee vara di
angle slighily truncate; beak sub-anterior, of moderate s
convexity, little elevated above the hinge line. — Se: a
Surface uniformly convex in the middle and anterior |
with a broad, shallow depression extending from the beak to
postero-ventral margin; post-cardinal slope with two strai ,
diverging, strongly projecting angular. ridges or folds, wii oat
tend to the postero-ventral angle, and are separated by a rounded, —

hae

ventrally deepening sulcus; posterior wing traversed by another Gr o fas
oblique and shallower depression and posterior extremity slightly Erin i
‘aised. Surface marked by equal filiform, concentric lines, which ao
on the anterior and middle parts pass parallel to the ventral
margin, between the post-cardinal ridges turn upward, and on
the posterior wing swing obliquely forward; these are crossed
on the anterior and middle parts by another system of vertical,
more closely arranged thread-like lines, which in smaller speci-
mens appear only between the concentric lines, in larger speci-
mens become continuous and more prominent than the latter.
Casts with a deep, backward curving impression in front of the
beak and a corresponding shallower, forward curving impression

ai i
oi
hy
4

r ae eee of Menace which, apne is known
1 casts; the casts of the two species differ materially i in the ©
. arater of the beaks, in the cardinal and general outline. Our
i species differs from all other congeneric forms whose surface
| sculpture is known, by its cancellate surface.

‘Upper Utica shales of northern Green Island, eee co. N. Y.

§ 3 ANNELIDA

Certain layers of the Utica eraptolite shales of the Rural ceme-
tery near Albany are profusely covered with worm-shaped car-
bonaceous films. The actual presence of organic matter, the
uniform dimensions of certain types and the distinct terminations
of the fossils leave-no doubt that they represent not mere tracks
but actual bodies of animals. Two types could be made out of
sufficient perfection to warrant their being named and described.

Eopolychaetus albaniensis gen. nov. et spec. nov.
(see pl. 1, fig. 13)

Head distinctly separate from the body, semicircular, with a
median oval depression which extends a little on the first body
segment.

of this worm could eS aE sah lished. witk h
clear that this type belongs to the class ol
this taxonomic date the generic term, E opulpeat
proposed for worms with similar, slender, eylindtic, 1 e
annulated bodies and long non-tufted setae on one sif
presence of another worm with setae was made known t
Ulrich, who found tufts of long setae in the Cincei:
(Jour. Cin, soc. nat. hist, 1878. 1:91). ati
Pontobdellopsis cometa, gen. et specs
fig. 14-18) . |
Body cylindric or rather long conical, regularly taper Py
abruptly terminating (with ring-like section) at wide ca
Other (anterior?) end provided with chitinous disk, the I 2
sometimes with central depression.
Segmentation coarse; 6 segments in 2.9 mm; segments § E
apparently not annulated; no appendages observed; test th ae TaN
(strong carbonaceous film).
Dimensions. Length of largest specimen observed, 11.7 om
and width at broadest end, 1 mm. ty
This small but common and characteristic form has been ng
termed Pontobdellopsis in allusion to its similarity to the
recent genus Pontobdella, from which, however, no close
systematic relationship of the fossil with that highly specialized
genus of recent worms is claimed.
The form is most common in the Utica shale of the Rural ceme-
tery near Albany, but it has also been observed in the lower

Utica shale of Mechanicsville.

: round at Balbous. and the .
eeu stout, blunt spine. The bay

; by fie. Pieiction of an elevated process, thus pao a separate
if io section of the species; in a very similar manner as the species
"of Ceratopsis, Ulrich (As Beyrichia oculifera,
Hall) differ from those of Tetradella by possessing an ele-
vated process. The remark of Mr Ulrich that these processes in
Cera t opsis (loc. cit. p.113) are not a “ mere ornament ” but
of a certain classificatory value, would be also pertinent in regard
to the two horned varieties of Ctenobolbina ciliata;
and it may at some time become necessary to unite them under
another generic name.
Dimensions. Length 1.45 mm, hight .80 mm.
Lower Utica shale of Mechanicsville, Saratoga co. N. Y. Up-
per Utica shale of Green Island, Albany co. N. Y.
2Ctienobolbina ciliata, Emmons gp. (see pl. 2, fig
a9).
Typical specimens of Ctenobolbina ciliata have been
collected at Green Island and at Menands (stations 10 and 11);

found in the middle Tite shales of Port Schuy er (sta
Valves shortly subovate, strongly convex, dorsal margit
straight; ventral part approaching a semicircle in ou Ai in 2 |
wide and deep, beginning near the middle of the dorsal m
oblique, curving backward below, dividing the car: ) ice in
subequal lobes, which are broadly connected in the »
region, the posterior lobe distinctly rounded and inclined |
little larger than the anterior; both lobes equally cony a y
thick (?) edge anteriorly and posteriorly; surface m
granulose. .
Dimensions. Length .56 mm, hight 57 mm, thickness a;
length of a smaller carapace, .48 mm, hight .34 mm, thi vo 20
mm. ery)
These minute valves are undoubtedly closely related to the t y
Trenton species of Ctenobolbina described by ma _
They fully agree with them in the presence of only one sulcus
which is strongly curved and of two bordered lobes; but they — t
differ from the one (Ct. fulerata) in having the posterior a
bulb already farther advanced, and from the other (Ct. crassa)
by the lesser development of the border and the shorter, more
rotund outline. Ctenobeltinn subrotunda differs
from Ct. duryi,S. A. Miller ep. (Cin. quart. jour. sei. 1874.
1:232), a similar form from the “Hudson river group” of Cincin-
nati in being relatively much higher and having the suleus more

medially located.

‘
:

HUDSON RIVER BEDS NEAR ALBANY 5TT

Turrilepas(2) filosus, sp. n. (see pl. 2, fig. 18, 14, 15).

In the lower Utica shale of Mechanicsville, two plates were
found, which in size, outline and surface ornamentation greatly
differ from the minute plates of Lepidocoleus jamesi,
associated with them in great number. Both plates, though of
different size, are so clearly alike in outline and sculpture that
they undoubtedly belong to the same species.

Plates obliquely subtriangular, comparable in outline to an
isosceles triangle with the apex pushed to one side; the nucleus
falling into the apex, and the two legs standing nearly vertical
on the slightly convex base; the lengthened side strongly convex,
the shortened nearly straight; surface marked by strongly ele-
vated, very regular concentric lines, which have multiplied more
rapidly on the posterior side.

Dimensions. The smaller specimen measures 4 mm along the
base, and 4.5 mm along the vertical side; the larger 7 mm and 9
mm in the same directions. ;

Both valves figured differ markedly from the typical plates of
Turrilepas by their outline, the absence of the sigmoidal
curvature in the base, their relatively larger size, and the char-
acter of the concentric striae, which appear not as the edges of im-
bricating layers, but as strongly elevated lines with deep, even in-
terspaces and by the conical shape which they probably possessed
originally; for they present the appearance of convex bodies
which became flattened in fossilization. This is specially dis-
tinct in the smaller specimen (pl. 2, fig. 18), where a median
furrow or break separates two differently convex halves. In all
these features they agree with another group of valves which
have been doubtfully referred to Turrilepas by Whitfield
(Annals New York acad. sci. 1882. v.2. no. 8. p. 217) and by
Hall and Clarke (Pal. N. Y. 1888. 7:219). The latter authors
remark “that it is difficult to see how the combination of
these subconical bodies in vertical ranges could produce such
a scaly peduncle or capitulum as existed in Turrilepas 6
and point out their resemblance with Spathiocaris. This
form (Turrilepas (?) newberryi), from which ours dif-

AVA aoa aa by a

cor

their possible crustacean sahiee led to the astc : ee ne |
that they all find their homologues in parts of the
the pedunculate cirriped genera Scalpellum ag
cipes, notably of the latter. On this acta
valves have been united under the caption, — Po
siluricus, in full consciousness of the enormous ¢ ral
ing between the appearance of this Lower Silurie typ “a I
next Upper Triassic (Rhaetic) representatives of these ren r
But the analogous case of the related Balanidae might be Pa:
in support. Charles Darwin, in his classic memoir on the fa
Cirripedia,* stated that in the sessile Cirripedia, or Bets ey
the negative evidence of their not being found in rimay =
secondary formations is of considerable value, consideeigiaa he ein

yet, meanwhile, nedoubted Palepatiie genera of Balanites (Protas
tobalanus, Palaeocreusia) have been found, leaving By :
the long interval from the Devonic to the Cretaceous without
any representatives of this family. It is an interesting query, .
What were the conditions of marine life that suppressed the Lepa-
didae and Balanidae, which today fill the oceans with such vast

‘A monograph of the fossil Lepadidae, or pedunculated cirripedes of
Great Britain. Palaeont. soc. 1851.

a scutal margin
ntly Berita aes ies as abe as the ce nee margin.
cludent margin and upper part of carinal margin meet at an

a angle of over 45°, gccludent and scutal margins at about 135°.
From the apex to the sharp basal angle, a strongly projecting,
3 angular, strongly curved conspicuous ridge runs at about one
fourth of the entire width of the valve from the carinal margin;
the surface slopes,apparently on account of lateral compression,
much steeper away on the carinal side. A wide depression with
a central, broad but low, slightly curved ridge extends from the
apex to the middle of the scutal margin.

The surface is covered with unequal, somewhat lamellose
growth lines, running parallel to the base of the valve. Where
the shell has become exfoliated, regular rows of pustules running
parallel to the keel become visible. These probably represent a
system of pores within the corium.

It is specially this valve that, in its outline, diagonal keel,
direction of growth lines and curved fold on the larger face, fully
agrees with the terga of some species of Pollicipes.

2 Carina. Lanceolate fragments are thought to have been
part of the carina. The fragment figured apparently had two
equal wings and a median, highly prominent, angular keel (an-

Be gS ees

The possibility bs this valve cae be’ a iat 01
and extenuated tergum is excluded by its pa: 2 ris
3 Rostrum. Small, thick-shelled, symmetric, for m ing
sides of a tetrahedron; apex incurved (flattened in tk
specimen by compression, as indicated by a break); k ‘Ss
elevated, angular, broad; surface with strong oneal g
lines running parallel to the basal margin. * s ss “
This valve bears a strong resemblance to the rostrum
licipes carinatus, which, however, has a flat-to pp iss
4 Upper latus. Small, little convex, six-faced, eig
thick-shelled; two middle faces forming a high, pasar

©
*

ie h
kel

te str

~< 7

keel; other fares nearly flat; surface with fine, concen ial ¢ Bic 1 th
lines; broad, concentric undulations, crossed by fine radial s tra me

on the two extreme faces and along the basal margin. om ste ie
This valve has been termed an upper latus on account of. its” a
similarity to the upper latera of Scalpellum quadratum
and Sec. fossula. The general form of this valve is very
much like that of some of the problematic Pt erothecas de-
scribed by Hall from the Trenton, and by Barrande from the
Bohemian Siluric. As our specimen however, agrees in the
nature of its shell with the valves of Pollici pes with which
it is associated and can be referred to a part of the capitulum of
this crustacean, it seems at present more profitable to unite it

with the latter than to compare it with the still entirely problema-
tic Pterotheca.

per latus: Reugihte 6. re mm, mpiditi 8 mm.
2] ‘Utica, shale of Mechanicsville, Saratoga co. N. Y. Upper

DESCRIPTION OF MAP

“The roman figures indicate the localities which furnished fos-
| correspond with the numbers of the stations described.
e boundary lines of the zones or belts have nowhere been ob-
ved directly; they are only approximations obtained from the
location of the stations. The location of the fault, separating
the Cambric and Normans kill beds, is taken from Walcott’s
map of the Taconic region (36).

REFERENCES

1 W. W. Mather. Annual report on the geological survey of the first
district. 1889

2 W. B. & H. D. Rogers. Physical structure of the Appalachian
chain. (Trans. Amer, ass’n geol. and nat. 1842. p. 474-581)

3 Ebenezer Emmons. Geology of New York; rep’t on the second dis-

triet. 1842 -

4 W. W. Mather. Geology of New York; rep’t on the first district.
1843

5 Lardner Vanuxem. Geology of New York; rep’t on the third dis-
trict. 1842 .

6 James Hall. Geology of New York; rep’t on the fourth district.
1843

i Paleontology of New York. 1847. v. 1

8 1859. v.3

9 EH. Billings. On the occurrence of graptolites in the base of the
Lower Silurian. (Can. nat. and geol. 1861. 6:344-48)

10 James Hall. Geological report of Wisconsin. 1862. p. 47 (footnote)

Graptolites of the Quebec group. (Can. org. remains. Decade 2.

1865)
12 H. A. Nicholson. On some fossils from the Lower Silurian rocks of
Y the south of Scotland. (Geol. mag. 1867. 4:107—13)

Vv Vv
ag? @ re

Pah oe ~ Toe

(Amer,
~ me a,

4 aa

+

Palachian range within
11:627-28)

WT
iw
’
.
’

4
¥ =

19 ©. D. Walcott. ‘The Utica slate and related formations of t

21

26

seological horizon. (Trans, Albany inst. 10:1-88) =

T. N. Dale. On the age of the clay-slates and grits of Poughk 20]
(Amer. jour. sci. 1879. 3d ser. 17:57-59) an

J.D. Dana. On the Hudson river age of the Taconic schists ant
the dependent relations of the Dutchess county and y iter
necticut limestone belts. (Amer. jour. sci. 1879. 17:375) ee

W. R. Gerard. The Hudson river group at Poughkee psie. (
naturalist. 1879. 18:199) » Aine at See

W. B. Dwight. On the recent explorations in the Wappin

~ limestone of Dutchess co. New York. (Amer. jour. sci. 1879.
17:389-92) a hy TH
Calciferous as well as Trenton fossils in the Wappinger |
stone at Rochdale and a Trenton locality at Newburgh N. Y. (
jour. sci. 1880. 19:50-54) a
Arnold Guyot. On the physical structure and hypsometry of the Ci

Catskill mountain region. (Amer. jour. sci. 1880. 19:429-51) ie Me
C. E. Beecher. List of species of fossils from an exposure of the
Utica slate and associated rocks within the limits of the city +}

4
*

a

=

of: Ke
Albany. (86th an. rep’t N, Y. state mus. nat. hist, 1883. p. 78)
H. Booth. Discovery of Utica slate graptolites on the west side of
the Hudson. (Amer. jour, sci. 1883. 26:380-81)
W. B. Dwight. Recent explorations in the Wappinger valley lime-
Stone of Dutchess co. N. Y. (Amer. jour. sci. 1884. 27 :249-59)
8S. W. Ford. Age of the glazed and contorted slaty rocks in the
vicinity of Schodack Landing, Rensselaer co. N. Y. (Amer, jour.
sci, 1884. 28:206~9)
Age of the slaty and arenaceous rocks in the vicinity of
Schenectady N. Y. (Amer. jour. sci, 1885. 29:397-99)
Great fault, Schodack Landing, N. Y. (Amer. jour. sci. 1885,
29 16-20) 7
N. H. Darton. Fossils in the Hudson river slates of the southe
part of Orange co. N. Y. (Amer. jour, sci. 1885. 30:452-54)

’
=
i

a
hoe

.

a.

51

52

oe rl E é 1888, 5. ao

“Gy D. Walcott. The Taconic system ae Emmons, and heh use of the

name Taconic in geologic nomenclature. (Amer. jour. sci. 1888.

“i 35:229-42, 307-27, 394-401, with map)

Value of the term “ Hudson river group ” in geologic nomen-
es (Bul. geol. soc. Amer. 1890. 1:335-57)

©. A. Ashburner. Petroleum and natural gas in New York. (Trans.

Amer, inst. min. eng. 1888. 16:1-54)

H. M. Ami. On the geology of Quebec and environs. (Bul. eee soc.
Amer. 1890. 2:478-502) | i
W. W. Dodge. Some Lower Silurian graptolites from northern

Maine. (Amer. jour. sci. 1890. 40:153f)
R. W. Ells. Stratigraphy of the ies group. (Bul. geol. soc.
Amer. 1890. 1:453—-66)

C. S. Prosser. Thickness of the Devonian and Silurian rocks in Bi

ern central New York. (Amer. geologist. 1890. 6:199-211)

J. P. Kimball. Siderite basins of the Hudson river epoch. (Amer.
jour. sci. 1890. 40:155f)

Bailey Willis. The mechanics of Appalachian structure. (13th an.
rep’t U. S. ‘geol. sur. 1893. pt 2, geol. p. 212-48)

T. N. Dale. The Rensselaer grit plateau in New York. (18th an.
rep’t U. S. geol. sur. 1893. pt 2, geol. p. 297-337)

I. E. Wolff. Geology of Hoosac mountain and adjacent territory.
(U. S. geol. sur., monogr. 23. 1893. p. 41-102)

C. S. Prosser. Thickness of the Devonian and Silurian rocks of Cen-
tral New York. (Bul. geol. soc. Amer. 18938. 4:91-118)

G. F. Matthew. Climate of Acadia in the earliest times. (Bul. nat.
hist. soc. New Brunswick. 1893. 11:3-18)
WN. H. Darton. Preliminary rep’t on the geology of Albany county.
(18th an. rep’t N. Y. state geologist. 1894. 1:229-61) :
Geology of Minnesota. 1895-97. v.3 of final report. pt 1 and 2,
paleontology.

R. R. Gurley. North American graptolites: new species and ver-
tical range. (Jour. geol. 1896. 4:63-102, 291-311)

T. G. White. The faunas of the Upper Ordovician strata of Trenton
falls, Oneida co. N. Y. (Trans. N. Y. acad. sci. 1896. 15:71-96)

C. R. Van Hise. Deformation of rocks, 4. (Jour. geol. 1896.
4:593-629)

a ne ee
. 4ES at me
ol (a ihe ~
ao 5° ‘ r Pd ‘ j
4 i rer epee
a it
oT

ped “1898. Ri A . sa aie aot ee ae is
59 F. C, Chamberlain. A systematic source of ra ition of ©
faunas. (Jour. geol. 1898. 6:597-609) _ eae es
© Stuart Weller. The Silurian Cisnnliniaeetad. on the epic nt
basis. (Jour. geol. 1898. 6:692-703)
61 R. P. Whitfield & F. O. Hovey. Catalogue of the t
specimens in the paleont. collection of the. geol. pia art., Am
nat. hist. (Bul. Amer. mus. nat. hist. 1898. v.11. pt ce
J. M. Clarke & Charles Schuchert. -Romencanong
York series of geological formations. (Science, sib Os
T. N. Dale. The slate belt of eastern New York and » si
mont. (19th an. rep’t U. S. geol. sur. 1899. pt3. p. 3 159-30 '

‘2

&

Leptobolus Ptootii Sp. n.

‘6 ie small perfect specimen; showing fine concentric striation.
Somewhat compressed. x6
7 An internal cast of a brachial valve; showing pone groove,
median septum and lateral scars. x4
8 The interior of a brachial valve, showing median septum and
lateral scars. x6
9 A very young specimen, partially exfoliated; showing radiat-
ing striation of internal surface and pedicle-groove. x10
10 A strongly concentrically and radially corrugated specimen;
the usual mode of preservation. x4
11 The interior of a similar specimen, showing pedicle-groove.
al
12 A shell, which instead of becoming corrugated, burst on com-
pression. x4
Normans kill shale of Mt Moreno near Hudson N. Y.

20 Surtase wlndaenieta see ine | cats a
21 Sperimen with Sietiel bsetSeboeie = Fe saa
22 Partial cast, showing the PEN on both

beak ke ae
23 Valve with nearly equally strong concentric and
lines

Pes, J

24 Largest specimen observed with somewhat aif el ‘ent 0
and stronger vertical lines |

25 Surface sculpture of the same. x6

PLATE 2
- Ctenobolbina subrotunda sp. n.

1 Right valve. x17
2 Ventral view of the same. x17
3 Another valve. x17
4 Ventral view of the same. x17
Originals of figures 1-4 are from middle Trenton shale of Port
Schuyler, Albany co, N. Y.

Ctenobolbina ciliata Emmons sp., var. cornuta var. noy.

or

Small left carapace. x17

6 Ctenobolbina ciliata. Larger right valve. x17
From lower Utica shale at Mechanicsville, Saratoga co. N. Y.
Ctenobolbina ciliata. Right valve

From the upper Utica shale of Green Island, Albany co. N. Y.
x17

Museum.

*

y State

N

42

‘

Teh
TOUR U Hilieh;

may Mh he

Lyre

lith.

Ast

Phil

rinter

S B. Lyon. State P

=

Jame

G.B.Simpson del.

i PLA

repr

hada,

nter

1
;

Pp

ran)
S

Stat

on.

es B. Ly

Jam

G.B.Simpson del.

=.

{

~

Pollicipes siluricus sp. n.

All figures enlarged three times.

Sayer Utica shale of Green Island, Albany co. N. Y.
o47 A smaller and shorter tergum from the lower Utica shale of
| Mechanicsville, Saratoga co. N. Y.
18 Carina .
19 Lateral view of larger carina. This valve has a prominent
lateral ridge and narrow marginal border |
20 Fragment of a carina with broad and low lateral ridge and
broad marginal border
21 Farther enlargement of surface of original of fig. 18. x8
22 Rostrum |
23 Lateral view of the same.
Originals of figures 18-23 are from the upper Utica shale of
Green Island, Albany co. N. Y. ;
24 Upper latus, from a gutta percha impression. Lower Utica
shale of Mechanicsville, Saratoga co. N. Y.

- observatory, 529°;

a

. hastatus, 546°, 5472, 5852.
Annelida, 573°-74°.

wi Aparchites minutissimus, 5211, 521°,
ia, oon.

Archinacella patelliformis,
a pata gar, 525°, 526, 527°.
rc _ Asaphus platycephalus, 503°.
vetustus, 5017.

Ashburner, C. A., cited, 5834, 560°.
Avicula trentonensis, 502+.

516’,

Balanidae, 578°.
Barrande, cited, 580’.
Bathyurus, 510°.
Beaver park, 530°.
Beecher, ©. E., cited, 582’,
525°, 526°, 5297, 564°.
Beekmantown limestone, 544".
Bellerophon bilobatus, 499%,
502, 520°, 525°, 527°.
- eancellatus, 493°, 502°.
Beyrichia oculifera, 575°.

5027-3’,

500",

569".

Black creek, Moathoesville. 531* -323.
Block island, Cohoes, 516-17.
Bollia, 545°.

Booth, H., cited, 582”,

Brachiopoda, 5697-727.

Brothers’s quarry, South Troy, 535°-
pees a

Buttermilk fall, Watervliet, 528°.
Bythotrephis subnodosa, 499%, 500°.

Cahill’s hill, South Troy, 5397.
Calciferous sandstone, 544".

Callopora, 547°.

ampla, 5457,

cf. ampla, 544°.

multitabulata, 545°.
Calymmene sp., 521.

senaria, 503°, 525°, 526".
Camarella hemiplicata, 5057.
Cameroceras proteiforme, 516%, 5174,

524°, 526", 5321, 532°.

Canada, graptolite faunas, 508°.
Canadian survey, effect on correla-
tion of Hudson river shale, 494*.

Cantonment hill, 546°,
Carinaropsis orbiculatus, 493°.
patelliformis, 493°.
Castleton, Moordener kill, 543°-44°.
Ceratocephala (Acidaspis) trenton-
ensis, 526".
Ceratopsis, 575°.

516°, 516°, 525°, 526°.
Climacograptidae, 498°.
Climacograptus, 542°, 547°.

bicornis, 4967, 497°, 502%, 502°,
529°, 530°, 539°, 540°, 541°, 5427,

44.
caudatus, 520°, 5215,
564°.
parvus, 523', 539°, 5411, 5444, .
scharenbergi, 541°, 547°, 585°.
typicalis, 523%, 524°, 526%, 529%,
530°, 531°, 532%,
Clionychia, 526°.
undata, 525*, 564°.
Coenograptus, 498,
gracilis, 528°.
Coenograptus gracilis zone, 506',
509°, 567%.
Cohoes, Block island, 516°-17'.
Cohoes beds, 498°.
Cohoes falls of the Mohawk river,
513°-16*.
Composite character of Hudson
river beds, 496°,
bed, of lower Tren-
ton aspect in shale, 544'-46°, 558;
on Rysedorph Hill, 546*-49°,
m4".
Conularia (Sphenothallus), 516°.
hudsonia, 520°,

Conglomerate

Conradella compressa,

Clsidicnharns piasviaden’ 408", 502, |

522%, 551°,

a SND
SE ee

duryi, 576". ae
fulcrata, 576", nett Be
subrotunda, 585%, 57 ee
ation of plate, Ber
Ctenodonta levata, won
Cumings, E. R., cited, 5 )
Cuneamya sp., 520°. *
Cyathophylloid corals, sor. S 4 Bie
Cyclonema bilix, 525°. ie *
Cyclospira bisulcata, 520°, 21, 5
Cyphaspis, 526°.
Cyrtoceras annulatum, 5207,
564°. GT
Cyrtolites ornatus, 516°, 525. :

sed
= a
“

Dale, T. N., cited, 582‘, 583°,
499°-500°, 511°-12", 5577, 560".
Dalmanella testudinaria, 515%, § ore
525', 526‘, 527, 534°, 5367, 545%,
Dana, J. D., cited, 582‘, 500°-2?, = +a
Darton, N. H., cited, 582°, 583°, 490%,

504-5.
Darwin, Charles, cited, 578°.
Dawsonia, 540°.
campanulata, 520*, 522°, 5417.

ras polyehastae Bis crass SSR Ree

albaniensis, 529', 573-745; ex-
planation of plate, 586’. fi

Ae Batt, os | Escharopora angularis, 536".

recta, 501’, 501°.

us zone, lower, see also

Figures, explanation of, 585'-88*.
Fitzgerald’s quarry, Port Schuyler,
5384-35*. .
Ford, S. W., cited, 582°, 5037-4°, 548%.
Fossils, discovery of stations with,
513; of Hudson river group, 490°-
91°, 493°, 5027, 504°-5*; Lorraine
beds, 493', 496°, 498", 513°-19°, 521°;

B10, 562°. —
raptidae, 498°.
, graptus, 5427.
tees ep., 5157.
—s ampilexicaulis, 4977, 5337, 535°,
Bao. er. DOU, Ooo", DOT, DOL’,

Sy Sei Normans kill shales, 4934, 496°,
a _ angustifolius, 541*, 544’. 496° 497%, 4987, 503%, 507°, 5387-50°;
"foliaceus, 497°, 516°, 517°, 517,| Prenton limestone, 499°-502", 505‘,
F 520°, 524%, 526°, 534°, 535°, 539°, | 5214, 533°-38'; Utica slate, 496°,
539°, 541°, 544°. 497%, 498°, 5022, 503°, 519°-33°; from

, cf. foliaceus, 531’. various stations, comparison, 551%-
-‘mnarcidus, 524*. 52': new, description of, 569-81’.
| mucronatus, 502*, 503". Frankfort slates, 492‘; correlated
pristis, 4967, 497°. | with Hudson river beds, 491%,
putillus, 498°, 514°, 515°, 516°, | 499°, 4958, 507°.
923%, 524%, 528", 528", 530°, 530°, | Frech, Fritz, cited, 584", 489°, 497’,
aot. 515°, 528°, 562°, 563°.
aff. putillus, 541°. French mills, exposure of Lorraine .
quadrimucronatus, 497°, 520%, beds, 518*.
521%, 531". Fucoides dentatus, 490°.
ruedemanni, 529°. lineatus, 490°.
spinulosus, 523%, 528*, 530°. ramulosus, 490°.
whitfieldi, 497°, 5415. sete abee
Discina conica, 501°.
Dodge, W. W., cited, 583%.
Dry creek, Watervliet, 517’.
Dudley observatory, 529°.

Gerard, W. R., cited, 582°.
Glenmont, 543°.
Glyptocrinus decadactylus, 514°.

511°, 514°, 528°, 534%, OT.
Guyot, Arnold, cited, 582%, 553°.

Hall, James, cited, 581", 581°, 582’,
582", 489°, 490°, 493"-96*, 500", 508°,
514°, 521", 525°, 528°, 5344, 536+,
536", 345°, 558°, 5644, 577%, 580°.

Helderberg mountains, te of
Lorraine beds, 518°.

Heterocrinus heterodactylus, 516’.

Hormotoma cf. gracilis, 529°.

Hovey, F. O., cited, 5844,

Hudson river beds, history, 490°-
512°; fossils, 490°-91", 493°, 5022,

*“D*, 549°; correlated with Lor-
raine beds, 491°; correlated with
Frankfort slates, 492%, 495°; cor-
relation with Point Lévis shales,
494°; primordial (Quebec) age of,
494°; composite character, 496°;
break between Hudson valley re-
gion and Mohawk valley, 504°;
evidence of Trenton age, 505°; cor-
relation with Trenton limestone,
O12; resting on lower Trenton
limestone beds, 549°; Trenton fos-

4; four zones, 550°-51°,

5OS*, 5677; explanation of overturn

of strata, 552"-5s8*: thickness, 5607;

Mohawk valley,

567°-GS*

river group, use of term,

402", 492°, 493', 493°-94";

sils in,

in the 565°; sum-
inary of paper,
Hudson

$91",

Gurley, R. R., cited, ot “50 4974, |

asked. » Ls cited 525%, 5s

Kenwood, 543, a
Kimball, J. P., Be 96

Lansingburg, not | end of,
42°; bluff above, 542.0
Lapworth, Charles, cited, 583", 584
489°, 4974, 505'-6%, 522", 528", 5:
562°, 5637, 5677.
Lasiograptus mucronate
Laveny’s point, Waterford, §
Lavery’s quarry, 5357. M3
Lepidocoleus jamesi, 516°, 521,
526°, 535'; description, BIT; =
planation of plate, 587°.
Leptaena rugosa, 525°. vane
sericea, 499°, 500°, 500°-1', 501%,
502%, 503°, 505°. ny;
subtenta, 502*, 525°.
Leptobolus insignis, 515°, 5204, 5214,
O24, 524°, 529', 530*, 531°, 570,
walcotti, 541°, 569°-70"; explana:
tion of plate, 585%.
Leptograptus subtenuis, 539, 543°.
Lingula curta, 508°, 515°%, 520*, 5214
Lingulops, 569*.
Lophospira bicineta, 526°,
uniangulata var. abbreviata,
525°, 526°,

Baie

eit eal

oy 525°.

y yuleheltum, 493°, 516°, 525°.

_ Marsouin river zone, 506%, 509%.
omatner, W. W.,

490°-927, 4997, 553°.
Matthew, G. F., cited, 583’, 562°.
Mechanicsville, 519*-23°,
Menands, railroad station, 527°.
Miller, S. A., cited, 573°.
Minnesota, report on geology, cited,
583°.
Modiolopsis anodontoides, 516.
faba, 516°, 526°.
modiolaris, 520’, 521°, 5227,
nuculiformis, 493°, 516', 516°,
. 520".
Monograptus serratulus, 496".
Moordener kill, Castleton, 543°-44°.
Mt Moreno, alternation of green
Slate with graptolite shales, 550°.
Mt Olympus, Troy, 540-41’.
Murchisonia, 559+.
gracilis, 493°, 502°.
uniangulata var,
520°, 526°

abbreviata,

Nemagrapsus capillaris, 528°.
elegans, 528°.
Nicholson, H. A., cited, 581°.

cited, 581°, 581’,

. Tees 507%; assignment: by. Teme }
York and Canadian geologists, ‘ee

508°; result of former investiga-
tions, 5127-13"; description of
beds, 5387-50°; conglomerate beds
of lower Trenton aspect, 544*49°,
558*; lower Trenton age, 510°, 511°,
512°, 547°, 567°; eastern repre-
sentative of part of the lower
Trenton, 557°-58'; taxonomic posi-
tion, 489°, 550°-52*; resting on
lower Trenton limestone, 550%,
558*; thickness, 560°; use of term,
566°, 567°, 568*; summary of paper,
567°-68*;

fauna: 498*, 496°, 497°, 4987,
503*, 507°, 538"-50°; correlated with
Lorraine faunas, 496°; homotaxy
with that of Utica shale, 497°;
lower Trenton age, 510°, 511°, 512%,
547°; European and Atlantic con-
nections, 510°; origin of, 562", 563°.

Normansville, 5307-31.
North Troy, 537’

Orthis (?) centrilineata, 515°.
Iynx, 501‘, 503°.
pectinella, 499°, 500%, 500°, 501°,
505?.
plicatella, 5057.
testudinaria, 4997, 500°, 500°,
502", 503°, 505%, 507°.
tricenaria, 500°, 501°.
Orthoceras, 501°.
bilineatum ?, 502°,
lineolatum, 525°.
tenuitextum, 525°.

Orthograptus quadrimucronatus,
514°, 527°, 528°, 580°, 531°.

522', 525%, 526%.
Plates, explanation of, 585’-88*.
Platystrophia biforata, 515°,
534*, 5367, 545°,
Plectambonites aff. gibbosa,
45°, 547°, 561".
plicatella, 520%, 521°.

sericea, 515*, 520°, 526°, 5274,
534, 536°, 564°.

var. aspera, 525°, 527°, 544°,
545°, 48°, 561".

Plectorthis plicatella, 525', 526*, 527‘,
534°, 536°.
Pleurotomaria cf. lenticularis, 525’.
Plumulites sp.?, 502%.
Poesten kill, South Troy, 539-40".
Point Lévis shales, 494*, 495".
Pollicipes carinatus, 580°.
siluricus, 521°, 526*; description,
578’-81°; explanation of plate,
5ST*-SS*.
Pontobdellopsis cometa, 520°, 529*;

description, 574°; explanation of
plate, 5867,

Port Schuyler, Fitzgerald’s quarry,
534’-35'.

Potsdam limestone, 544’.

Prasopora, 536.

Primordial (Quebec) age of Hudson
river beds, 404",

Pholidops subtruncata, 520%, ar aE *y

Rhynchonella pre ¥
Rhynchotrema incre’ ocke
Richmond stage, 566°
Roemer, Ferd. cited, 584’,
Rogers, W. B. & H. D., ‘ated,
5DAY. a
Ruedemann,
562°.
Rural cemetery, Albany, 5257204, Fe im
Ruscher’s quarry, South Troy, 537. ‘oh
Rysedorph Hill, conglomerate ede
546*-40°. . i

i &
a,
’
+

Rudolf, cited, co
.

pest 2
s a ‘ ‘
ea

\

Sagenella sp., 516".
ambigua, 532", 532%.
Sardeson, F. W., cited, 584°, 514°.
Sealpellum, 578‘.
fossula, 580’.
quadratum, 580".
Schizambon (?) fissus var. ria
sis, 529°.

. Sponge, 520°

Fe _Spyroceras bilineatum,

525°, 527°,
564°.
Stations, description of, 513°-44°.
Streptelasma corniculum, 544°.
Streptorhynchus filitexta ?, 505”.
planumbona, 505’.
Stromatocerium, 545°.
Stromatopora compacta, 501°.
Strophomena alternata, 499°, 500’,
5017, 501°, 503°, 5057.
incurvata, 525’, 544°, 545% 548°.
rugosa var, subtenta, 525’.
Summary of paper, 567°-68*.

Taconic, use of term, 494°.
Taxonomic position of the Normans
kill graptolite beds, 550°-52*.
Technophorus cancellatus, 525%,
572°; explanation of plate,
586°.
subacutus, 573%.
Tellinomya dubia, 502*.
levata, 502+.

Cana aie of ‘faunistic ‘sue
cession, 5615-642; of the Hudson —
valley, do not continue westward,
565%; | |

fauna: 4997-5027, 505*, 5214, 583°-
38, 562°; epicontinental origin,
510’, 563°; of conglomerate beds
of Rysedorph hill, 551%; in Utica
beds, 564°.

Trenton period, proposed term, 500°.

Triarthrus becki, 502°, 503°, 516%,

5213, 5267, 5321, 5637.

_Trinucleus concentricus, 502°, 505°,

(°, 515°, 516%, 5177, 518°, 5217, 5261,
5268.
Troy, stations, 5377; Mt Olympus,
540'-41?,
Turrilepas (?) filosus, 5217, 577'-78?;
explanation of plate, 587".
“newberryi, 577-782.
Typicalis, use of term, 523°.

Ulrich, E. O., cited, 5837, 500°, 506°,
536°, 536°, 546', 573*, 5744, 575°, 576*

Upper Dicellograptus zone, 5115,
522°, 567°.

Utica shale of Normans kill, 489°,

Utica shales, in the Hudson valley,
491°, 493°, 502°; homotaxial with
Normans kill shale, 492%, 497°;
Normans kill beds included in,
498°; testing, 519°; description, 519*-
33°; thickness, 560"; discontinuity
of faunistic succession, 561°-64?;

Viy, Serene along, 517-48 Voor:

heesville, 582-33... = .
gras ge soni Black creek, soe |
y, 532°-33'.

Walcott, C. D.. ie ae
490°, 498°-99", 50m, 507-8, 514,

3
:
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