- * * * : * * *, *
ºº::::::::::::…º.º.º.
ºs. sº
.*.*.*.*.*.*. ºf rºt & gº sº
º * - - - - - sº º
* * * * * * * : * . ->
* *** * *
º C
:::::: º:
& , *, *. 3 * * * * sº ºr
- * * * * * * ***** * * & ſº º º
º: . . *.*.*.*.*.*.*.* tº º º
sº. º * * * * * * º º, º º sº sº
sº sº... *.*. * * * º º
- º," "...º.º. - sº Fºº ***** Sºº
§º. * * * * -* - Wºrs {} -
*.*.*.*.*.*.*.*.*.* * : * ~ * * ºr * * *
Sºº','...'..." sº sº."
º : ºº e ºs sº
Kº
**_º - sº ... •
ºšº ºr
; : * tº sº
R" º
º * g a
& © e : * *
º
º
**, *, * : * ~ *
ºº::
ºf sº
º º
*...* Kºssº
"...º.º.º.º.
2 * * * * ºº::
..".º.º.º.
* * * º
** * * * : *.
Sººº...?
w ſº stºº gº
* * * * * * ſº a '• , as a
sº Cº. * * * * *
* * ** * *
sº :
º
* * * * * *
ğ º •º º ºf, * * *
º sº sº - Rºčº
ºº:::::::::sº. * * *
ºº:::::::::::tº º's & sº gº."
** **** :::::::::::::::::::: * * * * *
ºr ºr a a .
:::::::::::::::::::::::::::::::::::::::
Ç C *:::
& gº
º-º: Fºº º
r º f is a sº º sº. sº * tº
ºº:::::::::: º * * * *
Yº...”. * * * * *
º: ºr -º a
* * * *g
º
º
** *
º
º
sº
& gº º
º
º
º
iº
#
º&d
º
&
§.
* *
º
&º§º
º
º
º
º
º
:
§ºº
§
§
º
ſº
.*
:
RE
º
º
º
* 8
sº
§
§
* . & ºr tº ºc
..º.º. -- ~,
* * * * * * & ºr *
º:
º
sº-
... .".
** = … • s - .
*** * * *
º ºg
ſº
º
º
dº
: S v & º
* º ** = ºr
§§ E- º
-º-ºººº sº º
ºr ºf ººº-º-º-º:
-º-, -º-º-º:
tº:
º ſº rº
º ºgº sº
* - sº
gº º º sº
3 $ººs; º º
sºvº ſº ::::::::::::::::::::::::::
Q º
:::::::::: §:::::::::::::::::::::::
º
§: º
º
º º;
*ſ, *@ º 'º y
º: º:::::::::::::: y sº
ºº:: * * * * * * º
sº tºº :::::::::::::::
~ alsº
:::::: º ºº::
Rº: *** * * * * º ºgº
º ºº:: º º Ǻ
.*.*.*.*.º. ºf::::::::::::::::::::::: º
§ tº:
§:
** º sº Fºº
pººl º
sº.
º º
º ſº ſº
º Sº & ºrgs º
Ǻ º sº º º Sºº-
º:::::::::::: *ºrg º
sº sº º
ºttº: º
sº º sº : º
ºº:: Cº.
#
§:
Rºoseº
º:
º
º
Sºº ºrie ºg
Cºaº
tº º sº
º º
º:
º ºssº
º gº sº.
º ºº::
º::::::::::::::
;: ºº:
º
ſº
Rºº.
º
sº […] º fººt
[…º -
º
* º º &P c.
Cºº - º º ºxg s
** * * * º Kºsse *~ *-s re-es:
**s sº º - Sººtºº ºº::
§: §
* * º tº gº º' tºº...,. º
D º * = . ..º.º.º.º.º.º. º;
§ ºš :
º sº bºrº ES ºw sº §
Fº Rººs fºre
§: º: ºº::
º sº sº & º º
§: º tºº
**º ***s, sº
Xº sº
º ºº tº ºsº
sº sº E. º
ºnes ºrsº -
gº }
º
Fºr º: "...º.º.
ſºlºssº...º.º.º. ****
Rººse---...-a, -
º rºs º: *S** -ºgº *
**º
º a sº
º º ºgs tº
º º º
º º º º ſº º
> º ºg º
::::::::::::::::::::::: gº º
º
r ºfºº
º º
º
º
tº a
º
º º
£º
º º
ºtes *::::::::::::::: º
º º º iº
º
ğ º ºg ſº
º
ºw wº º
sº
º:
as ºne. ſº
º º Ç
ſº
;
º
º
*ºg º –
º
º
º
:::::::::::::::::::::::::::
º tº:
º
Rººg sº
Q & s
º
º
- º º
º sº º º
º tºº gºsº
º tº sº
º º
º
*** *º-sº
º
º º
Ǻ º º ºr ºr sº
Rºº. * : * ſº
:::::::::::::::::
º Sºº
gº;
ºilº
tº º: º
º º
fººtºº º
sº º º:::::::::: º
º tº ºr º º: ºrºgº lºss sº
** = g
º, Aº ºw sº *sº: º
...’sº tº sº.
º *.*.* -
º
º º
ºf sº sº
º
º Sºº
Pºº sº
&º º ſº
º Ǻ
ºr sº gº
º º
º ** **-º-º:
ºº::º:
*º sºng º jºseº.º.
tºº º
ſº º Hºº-sº º
º C
zºº - ºg
ſºgiº
ºe sºººººººº.
ºº::
$ºssrºeleº
rºsº º * -º cº º
* ºr re. wº
ºsº º
* * * ºr º: &
º ºg tº §: ****
Fº º º º
*Geº. º ſ
º º º ºº: ſº
tº ººzºº ~ sº º-º-º: - « . º
*.*.º. ºº º :::::::::::::::::::::::::::
ſº º tº º Bºaº
* Reº tº: toº * * * * * *** -ºº: Rºxie
gº.º.º.º. Pºiº ** **** * & tº *** * * * * ſº º
º, "... sº &ºg tºº ºf * * * * ::::::::::::::::::::
C. º,','º', tº: º; 5.º.º.º.
… d & *&# * gº º º º_* ...,
º • * - ºllº C = w º Sºº
K gº º tº ºt º º
ºº.
º
> -º
sº º:
*** *** -º º º ſº tºº
* <ºr ºf s - º ºt
** [… sº sº º º
* * *g, * * -º - º
ºº:: gºº's sº & sº
sº ºra, ºsmººr. ºssºs.sº sº reº.
ſºººººººº-ºº: Yºº.
§ &ºre ºg º º:
º * * * * * * ** a sº gº º º Sºº -º ºf sº sº
spºrºsº Sºsº sº º º
* Bºº ſº $º
fº sº
º sº
* Rºsº sº
rººrºº
sº -
ſº
Fºº
º:ºgº
* * * :
º º; tº-3
º
He tº ****** -ºº sº
* * *rººrºº
º
º
º
º-ºº: §§
sº º
jº
&
ſº
ſº re-º-º:
ºº: ººzºº erºs
$º: ºf sº wº
* * sº º º
º º º º:
is sº º º º
º Pºlº sº
ſº as ºr
iº º º [… ºr sº.
; sº Rºanwºº Rºß * º
** * * {{
º º
º Pº § º'º e º 'º sº
Rºº. ºº:: sº *>
sº: ºº: º
º - o *º
º ſº º º º ~ Sºº {
{º º: º º ºº:: º º
#::::::::::::::::::::::::::::::::::: ºº::: tº kº
º R
Sºº ºss ºr easº aw º º
ſº º º tºº
º º
º §:
§: sº
º
* gºº
º ** *****
ºr tº sº ſº -º-º: - & º º ºws ãº
º - = sº as º - º º
ſº w º º - º ºf º-
ºº:: º º
º Fººd º
º- ºrg
º *ě 'º -º
: § º:
º º
--- w - **:
*, *ºtºs º ºs º º ºº: sº º
x - º º: rowsº - ºº: * * ºr “sº - sºlº tºº
º º” . ::::::::::::::::::: - º: º º, º
ºrs º º *º º º º º ºg º º º:
º ſº - & # * ſº º
ºº::::::::::: º º º º
º
º tºº. º tºº ºr 2 ºf *º º *** - ºg
º º: Fº sº ğtº tºº,
º §::::::::::: ſº º {ºº
º º
º “º sa ºrg. º
º g º
is , º, a
º
sº ºº::
ºº: º
tº a - - -
* 4 * - & ºw. §º
2-2 rº *& tº: º * **** º - ſº
º sº rºº sº º J -
º
º º
ºreº.º.
sº
* * * *... ::::::
*** * ~ : * ~ *
* * * * * * * * =
º" ºf
* -ºº º
*** **
†:
sº Bºº
º zº tºº
..",". sº
º
** * * * * * * * * Sºº
tº
a º
E
*.*.*.*
* @ -
º sº -, * * * *
& sº sº º ºx º ºs º ºs
Fºr-º- º
º
º,? º:
** * * * * * * * * * *
º a sº -g = < c * * * * * rººs s.
jºsº, sº º ºs:
tº ºs y * * * * * *
º Tºº ſº ſº *
º º º
Cº- * * * ****** **, *
* * * * * * * * * * * *, *:
* * * * -
* - c **
& º . -ºš º sº tº ...
tº a 4-sºº. .
Bºº.
ºº:
* * * *
*.*.*.*, * ~ *.
ſº sº.”. º
"ºs"sº,'.
ºº:: * * * * * s
- --ºº:
sº º
* * * * * * * *
* * *-* * * * * * * *
• * * * **, *
tº gº. º ** ****
§ º - - gººs - a
ºº:: S-5'...º.º.º. * (* *.*.*. * * * : * ~ *
ºº:: Hº º º ** *** * g.º.º-º:
* * * * & B P - ſº * * * * * * * *
* * g =
* * * : * * * * **-* ~ *-*.
* * * * * * *
sº
* * * * * * * * * * * *
** * * * * * * * * : *
º “º * gº
** **** * * * *
* * * * * * * * * * * * * * * * * > * >
* ºr wº ºr * * * * * * * * *
º
º “ & 8
* * * ***
* * * * ~s
ºfºº
º ºgº ºr * * * * * **** * *
ºº:::::::::::::::: * * * * : * > *** - g : * : *
* : *º-sºvº. f = ′ ºr sº
- Sºº -e-…- …
tº c.a. sº * * * * *
º w
** * * * * * *-*.
gº * * * * * *…*.*.*.*.*, a
ºlºrs sººº-º-º: sº
Sºº - e º sº.a.
º:
º
ºr tº sº.
Sº sº...alºs
º
ºº: sº
sºlº º
*** ***** **** *
º ºr see rºº tºº
* * * ********* *.*.*.*.
º
º º ºsº
*** * * * * *
:*****º-sº sº sº a
* *º-sº
º “tº
sº wrf
º
* : * * * * * * º
w * **, *, * * * * =& ſº.;
Amºº ºº
*º-w ºre
* * * * *
º sº
ºº:
***** assis º.º. * * * *
ſº a ess satºs
&gº 3. ºr tº ºs.
tº: º
º
ºf ºs
º º
º sº
º sº
ºre tºº º º ºº: tº ſº.
º tº 4. ſº sº ºw ºs
#º * * * ºsºft
º Fº
§
:
ºſº
º
e
tº a
gºeºs ºjº
º
º
Nº.
rºss ºf
ºre sºaº sº.º.
* “Pºrsº "e
sº º, º ºs
º º &
gº º
º ºgº ºsº
º
º Sºº
º “* * * * ſº ſº Nº.
* * * * *g
:
º º Fº
- ºf ºw
- c ºº sº º
º g - w d - Sºś sº tº:
º - º fº.º.º. sº º º
º Pº wº ſº º
º:
ºº: - º w
º gºº:
ſº sº. º Sºº º
ºr gºes º
ºrs º: Pºrs ſºrºs
* º
º *Yºº gº
º º
gº
Jºº sº: Sº sº.
ºrs cºe º
º:
ºwº ºr sº º º
º tº sº? º
ºº:: sº sº
º º * wr
£º º:::::::::: Bºstº
rwºº º º
tºº º
~~~~ º º sº ::::::::::::::
º sº º: º º
sº * * * * * º º
º ºgº $º º º “ººsa is º -
º sº
- º
Sºº.
fºº
ºº:
º
º º w
sºº-ºº:
&º
º º ****** º
º º º
º:
ºº:: *
3&2& ſº gº
rººgee sº. Bº
E. sº
º §§ º
*** * * ºw º
º 'ºe -s ºf . ſº * º
º: º º:º: iº º ºº:: º º
º º * † ºf ººk ºº: º E
º º: Yº: - * *** ºtºs º
º “º º º - - w
g º 2 tº sº º ſº tº º sº.
É º tº:
º Sºº
* †º º
º º º * * * * sºlºs
º
sº
*... ... dº gº
***** * * *** -
aºerº.s.
* * * * *
º
*ge &
ºr sºrº.
º
ºr sº Sºº-ºº-ºº:
º ** º
Nº.
º
º
* ºf ºs ºs.
* * * >g a
ſº * * ºx
zºº º
ºxº
º
rººs
**** * *
Sºº
lºgº ºes
;
º
º is ºp sº
§ º F iſ . . . .
º * * * *
tº "...
ſº £º º *...ºggº. -
º
º
Hººgº
ºiº
Sºº-ºº:
º sºtº: ſº
* º ºgº
- º - - º Fºº º
º . ~ - º ºrce - º
º º $. *** * * º crº- º *ºss Kºz. .
ºº: º ºr º - *** *-4 º º º:
º
&A
&
º ºg
* - ſº º -
º sº Mºº
$ºse Fºº
****º
Öº
º ºgº.
ºr sº
º
ºrºg.
Kºº.
rºº ºf -
jº. º
yºkº a w º ºº:
e-º-º-º: gº',
ºf rºg sº sº ***** *
º ºgº º - tº wº *º
dº sº
ºſ-
sº tº tº sº sº
Rºe sºrº sººn
º: - º
º “wº sº. * * * *
* * g º ºs ºº::sºn * *g
ºwº º º
ºº:: tº º
R. v. ſº as ºr sº .*
º *** * * * *g. ſº
- Nº.
sº º:
º
ºº::
º º
º º º:
*sº º: º
º “º sº ºf * : º º º
º ºsº.'s º &
sº sº exas º: tºº s' . . .”
ºxº sº ºr º
º, º tº ºº:: s.sº, {
ºrgº sº ~ - *-ū .
tº gº º tº: º; :::::::
º # gº tº ºntºº y
ºº:::::::ff. sº ºº::
sº *_* ºf
º
$º
º
* exa
º
º
ºf Sº
ºr sºlº ºlº
º ºr sº. gº w śrºtºº
tºº º ºg º * t tº:
º”.º.º. º.º. jºx
jºº Y.".º: ***ºffs
º º;
§ º
ſº
exx. º º
tºº sº. E
tº sº." sº sa, - ſº º º d
sº tº: g ºrº Ł ºº Rºº-ºº:
º ºº e º sº dº - tº - sººººº-º-º: º
º: º “º º
*º & A. sº º: º º { zºº º
º
sº
3 º
º
º:
wº
& sº
º
º
tº sº
gº
sº
º Kºº-ººººººs.
º º: sº
º º º
g º º º
*** *** * * * º º zºº
ºº:: ..", tºº * Nº.”. ºº:: *~
ºf ſº tºº tº ‘s o -
º
º
ºf- º
ºº:
º
Sºº-ººººººººº.
º ººr ºº * * *
º: ºrcº º º: —ºº
Rºssº.º.º.º.º.
º sº ſººººººººººº.
gº º: & - sº Rºsº ºRºº. .
º: *> º º º º ***** * Yºº º -- ~~ - -
º º (º ; F = --> º - -
º: †: º §§ Cº-ye - sº tºº
º g -
&
§
.
|
2.
:§ 4
:
.
:
º
*...*.*.*.*.*.
º:S & Sº
º: S.
[.
&
- º
º
*.
sº § sº
º
º Nº.
º
Yºº
º & º -
&
*ºº º ºº. ****
§§
º º ºg Rºss º º - º
º º sº sº
§ §: Sº º º & º & §
&
*** º º
º sº - ºº::...sº
º * ~ º ºw
§ §
º S § tº
sº & º
º ...? º -
º N º sº º *.*.*.*.*. - -
3& § §§§ l
º [. kº- - * - & “º. º 3 ** :
º § º sº s
º § sº
º s
SS
Š
§ ãº,
- º
º §§§
§§ §
* Sºrº
ºšŠ
. sºlº
º
s *
sº
§§
º
iſſºn, - sº &
º & Sºs -
|
>
º
f
- ...; º
lºº. "
ºf "APA,
#:
nºr. Anot § º
UAERIS'PE M.AMOENyº, ºf
Q Tº NINSULA 2 * * §§ º -
Pº Sº Nºſ/ſilº
Jº
§
#!
(# E () L () (FY
OF
N E W - Y () R. K.
PART IV.
COMPRISING THE
SURVEY OF THE FOURTH GEOLOGICAL DISTRICT,
BY JAMES HALL.
ALBANY :
do e s s ºr se e
The copyright of this work is secured for the benefit of the People of the State of New-York.
SAMUEL YOUNG,
Secretary of State.
...Albany, 1843.
Tº 54.964
TO HIS EXCELLENCY
WILLIAM G. B.0 U 0 K,
GOVERNOR OF THE STATE OF NEW-YORK.
SIR,
I herewith submit a Report on the Geology of the Fourth
District, comprising the counties of Wayne, Monroe, Orleans, Niagara, Seneca,
Ontario, Yates, Livingston, Genesee, Erie, the western part of Tompkins,
Chemung, Steuben, Allegany, Cattaraugus, and Chautauque.
I have the honor to be,
With great respect,
Your obedient servant,
JAMES HALL.
P. R. E. F. A {} E .
HAVING been appointed by the late Governor, the Hon. WILLIAM L. MARCY,
to investigate the Geology of the Fourth District, which embraces the coun-
ties just specified, my duties in that region commenced in the spring of 1837.
The subjects of the successive Annual Reports since that time, are embodied,
as far as possible, in the following work. A multitude of minor details are neces-
sarily omitted, but it is believed that everything of economical importance has
found a place in this Report. -
I have conceived it my duty to record my own observations, rather than to
compile from the labors of others; yet it has been far from my intention to
neglect any sources of information within my reach; and at the end of the Re-
port will be found a list of those persons, so far as I know, who have written
upon the Geology of Western New-York. º
In the commencement of the work, it was intended to confine the details chiefly
to physical geology, and to present only a few of the most prominent and cha-
racteristic fossils of each rock; but, as there appeared some doubt whether the
work on Palaeontology would be completed, more attention was devoted to this
subject, and a large number of figures prepared for the work. Too little
time, however, remained for its proper investigation, and the descriptions
have been mostly written and the names given while the work was passing
through the press, and it would be presumptuous to suppose that what is done
can claim perfection. In preparing this part of the work, I have consulted all
the authorities within my reach ; it was undertaken both for my own benefit and
for those who wish to know something of the fossils of the New-York rocks, and
GEOI. 4th DIST. 2%
viii PREFACE,
who have not access to foreign authors on the subject. I feel, therefore, that
those who are the best qualified to judge of it, and to detect the errors, will
appreciate the motive, as well as the difficulties encountered, and deal leniently
with the faults.
The drawings for illustrating the organic remains, have been chiefly made on
wood by Mrs. HALL; and although I may be regarded as a partial judge, it is but
justice to say that they are executed with fidelity and precision, and the figures
will enable any person to identify the fossils of Western New-York.
During the first year of the survey, I was assisted in the field labor by the late
Dr. G. W. Boyd, and subsequently by Prof. E. N. HoRSFORD of Albany, and
Prof. E. S. CARR of Castleton Medical College. To the industry and fidelity of
these gentlemen it gives me pleasure to bear testimony; and to the first, who is
now gone from among us, I may be permitted to offer, in honor of his memory,
a tribute to his zeal, perseverance and accuracy. My acknowledgments are also
due to Mr. John PATTERSoN, of the Assembly Printing Office, for the careful
supervision of the sheets of this work as it has passed through the press, and I
have often had occasion to avail myself of his literary and scientific acquire-
mentS.
To THE INHABITANTs of THE FourTH DISTRICT, from whom I have received
the most liberal aid and encouragement, and to whose hospitality I have been
often indebted, I have many acknowledgments to make. It has been my first
endeavour to elucidate the geology and the economical resources of that por-
tion of the State; and if much time has been occupied in investigating the
lithological variations, the points of junction of successive strata, and especially
in obtaining great numbers of their characteristic fossils, it has been with a
view to carry out the plan of the survey in the spirit in which it was conceived.
The subject has been pursued throughout with a feeling that though utility was
one grand object, yet science was not to be subordinate; that in the Geo-
logical Survey of New-York, knowledge was to be acquired and disseminated
among the people, not only to aid them in understanding phenomena immedi-
PREFACE. - ix
ately connected with their pecuniary interest, but to direct them in gratifying
the wants of a higher nature, and appreciating the wisdom and beneficence, and
the harmony of design, in all the creations that have preceded, as well as in all
that now surround them. I cannot but believe that the organic remains presented
in this report, and which are so widely distributed, and so abundant in nearly all
the rocks, will be found an interesting subject of observation. To all young
persons, and to pupils of schools and academies, they will become a fascinating
study, and at the same time induce recreation and exercise, promoting health
and happiness.
Many points where I had promised myself a further time for investigation,
I have reluctantly been compelled to abandon. To have been able to review
many portions of the district would have given me pleasure, but the close of
every season has found me leaving the field only after the snows of winter
admonished me that I could no longer labor to advantage.
The enlightened spirit in which this survey was directed, and the munificence
with which it has been sustained, have afforded every means required for its
completion. The State of New-York, which has heretofore established her
claim to the dignity of the Empire State, has now added another wreath to her
laurels, in becoming the first in the patronage of science, and in the benefits
thereby bestowed on her citizens, as she is first in resources, in commerce, and
public improvements. - - ... '
Under such circumstances I offer these results with diffidence, conscious that
neither limitation of time, nor of expense, can be urged for the imperfections, and
none can feel more than myself the deficiency of the present report as an illus-
tration and description of the grand physical and geological features and phe-
nomena of Western New-York. But the field widens as we advance; as in
every department of nature, examination leads to more extended discoveries,
so the geology, and more especially the palaeozoic geology of every country is
a progressive study, offering to the student treasures ever new and in exhaust-
less variety.
JAMES HALL.
TABLE OF CONTENTs.
LIST OF ILLUSTRATIONS.
DESCRIPTION OF THE MAP.
PLAN OF ARRANGEMENT IN THE STATE COLLECTION,
CHAPTER I.
PAGE
PRELIMINARY CONSIDERATIONS • - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - 1
. CHAPTER II.
General features of the strata, topography, etc. of the Fourth Geological District. . . . . . . . . . . . . . . 12
CHAPTER III.
Tabular view of the rocks and groups described in the Geological Reports of New-York; their
extent and agreement with the formations of Europe. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 17
CHAPTER IV."
Enumeration of the rocks and groups (in the New-York system) below those of the Fourth
Geological District, in their order of succession. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 26
1. PoTSDAM SANDSTONE . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 27
2. CALCIFEROUS SANDROCK . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 28
3. BLACK RIVER LIMESTONE GROUP . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 28
4, TRENTON LIMESTONE . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 29
5. UTICA SLATE. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 29
6. HuDSON RIVER GROUP . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 30
7 and 8, ONEIDA ConglomERATE AND GREY SANDSTONE . . . . . . . . . . . . . . . . . . . . . . 31
3%
XII
CONTENTS.
Description of the rocks and groups of the New-York system, embraced within the Fourth Geolo-
9. MEDINA SANDSTONE
10.
CHAPTER W.
NEW-YORK SYSTEM.
gical District. . . . . . . . . . . . . . . . . . . . o e o O © e o 'º e o e º e º e º O e o O & e e C . . . . . . . . . . . . . . . . . . . . .
1. Red marly or shaly sandstone....
2. Grey quartzose Sandstone. . . . . . . .
3. Red shale and sandstone... . . . . .
4. Greenish-grey argillaceous or sili-
ceous sandstone. Grey band of
Eaton . . . . . . . . . . . . . . . . . . . . . .
Diagonal lamination . . . . . . . . . . . . .
Accretions . . . . . . . . . . . . . . . . . . . . . .
Localities. . . . . . . . . . . . . . . . . . © e º 'º
Thickness . . . . . . . . . . . . . . . . . . . . . .
Mineral contents . . . . . . . .
Springs . . . . . . . . . . . . . . . . . . . . . . . .
Agricultural characters. . . . . . . . . . . .
Organic remains . . . . . . . . . . . . . . . .
Ripplemarks. . . . . . . . . . . . . . . . . . . .
Shrinkage cracks . . . . . . . . . . . . . . . .
Sandy beach and stranded shells.....
Wave lines . . . . . .
e & 6 @ e º & © e º O e e º 0
CLINTON GROUP . . . . . . . . . . . . . . . .
1. Lower green shale ... . . . . . . . . . .
2. Oolitic or lenticular iron ore . . . . .
. Pentamerus limestone of the Clin-
ton group . . . . . . . . . . . . . . . . . &
4. Second green shale . . . . . . . . . . . . .
5. Upper limestone . . . . . . . . . . . . . . .
Localities. . . . . . . . . . . . . . . . . .
Thickness . . . . . . . . . . . . . © & © & © tº e º 'º
Mineral contents of the group.......
3
Organic remains . . . . . . . . . . . . . . . .
Localities of superposition..........
11.
NIAGARA GROUP. . . . . . . . . . . . . . . ©
General features, extent, etc. ........
1. Niagara shale . . . . . . . . . . . . . . . .
2. Niagara limestone . . . . . . . . . . . . .
34
36
37
38
39
40
41
42
43
44
44
45
46
49
51
52
54
59
60
62
64
65
66
66
67
68
78
12.
Sulphuric acid . . . . . . . . . . . . . . .
13.
14.
15.
16.
17.
18.
79
80
81
84
19.
20.
21.
Concretionary structure. . . . . . . . . . .
Topographical features............
Localities. . . . . . . . . .
Thickness . . . . . . . . . . . . . . . . . . . . . .
Mineral contents of the group. . . . . . .
Springs ... e e º e º 'º e º 0.
Agricultaral characters . . . . . . . . . . . .
Organic remains ... . . . . . . . . . . . . . .
ONONDAGA SALT GROUP. . . . . . . . . .
Subdivisions. . . . . . . . . . . . . . . . . . . . .
Localities. . . . . . . . . . . . . . . . . . . . . . .
Shrinkage cracks. ...
Minerals . . . . . . . . . .
tº e º e 9 º, º Q tº Q @ º
e e º ºs e o e º 'º e Q e e
Brine springs or Salines . . . . . . . . . . .
Agricultural characters. . . . . . . . . . . .
Organic remains. . . . . . . . . . . . . . .
Localities of Superposition. . . . . . . . .
WATERLIME GROUP ............
General characters and localities . . . .
Organic remains. . . . . . .
© & © e º ſº e g º e
Waterlime or hydraulic cement-...
PENTAMERUs LIMESTONE..
DELTHYRIS SHALY LIMESTONE...
ENCRINAL LIMESTONE...........
UPPER PENTAMERUs LIMESTONE..
ORISKANY SANDSTONE ...........
Its development and localities in the
Fourth District . . . . . . . . . & © tº e e
Organic remains .....
CAUDA-GALLI GRIT ...... & © e º O C e e
SoHoHARIE GRIT ................
ONoNDAGA LIMEstone...........
32
86
96
96
97
98
99
99
100
117
119
132
133
134
134
134
136
. . . 137
139
. 141
141
142
. 142
144
. 144
145
145
146
146
147
150
151
151
CONTENTS. - XIII
22,
23.
General features . . . . . . . . . . . . . . . . . 151
Localities. . . . . . . . . . . . . . . . . . . . . . . 156
Thickness . . . . . . . . . . . . . . . . . . . . . . 157
Mineral contents . . . . . . . . . . . . . . . . . 157
Organic remains . . . . . . . . . . . . . . . . . 157
CoRNIFERous LIMESTONE . . . . . . . . 161
General features . . . . . . . . . . . . . . . . . 161
Subdivisions . . . . . . . . . . . . . . . . . . . . 161
Localities. . . . . . . . . . . . . . . . . . . . . . . 167
Thickness . . . . . . . . . . . . . . . . . . . . . . 168
Mineral contents . . . . . . . . . . . . . . . . . 168 -
Springs . . . . . . . . . . . . . . . . . . . . . . . . 168
Agricultural characters . . . . . . . . . . . 170
Organic remains . . . . . . . . . . . . . . . . . 170
MARCELLUS SHALE . . . . . . . . . . . . . . 177
General features and extent......... 177
Localities. . . . . . . . . . . . . . . . . . . . . • e 179
Thickness . . . . . . . . . . . . . . . . . . . . . . 179
Minerals . . . . . . . . . . . . . . . . . . . . . . . 179
Springs . . . . . . . . . . . . . . . . . . . . . . . . 179
Agricultural characters. . . . . . . . . . . . 179
Organic remains . . . . . . . . . . . . . . . . . 180
Localities of Superposition . . . . . . . . . 183
24. HAMILTON GROUP. . . . . . . . . . . . . . . 184
25.
i
. Dark slaty fossiliferous shale ..... 187
. Compact calcareous blue shale ... 187
An olive, or often bluish fissile shale, 187
Shales of Ludlowville . . . . . . . ... 187
Encrinallimestone . . . . . . . . . . . . . 187
. Moscow shale. . . . . . . . . . . . . . . . . 187
Joints or vertical cleavage ......... 192
Concretions. . . . . . . . . . . . . . . . . . . . . 192
Localities. . . . . . . . . . . . . . . . . . . . . . . 193
Thickness . . . . . . . . . © e º 0 e o e º e o o e e 194
Mineral contents . . . . . . . . . . . . . . . . . 194
Springs . . . . . . . . . . . . . . . . . . . . . . . . 194
Agricultural characters. . . . . . . . . . . . 194
Organic remains . . . . . . . . . . . . . . . . . 195
Localities of Superposition ......... 211
TULLY LIMESTONE . . . . . . . . . . . . . . 212
Extent and general characters ...... 212
Concretionary structure............ 214
Localities . . . . . . . . . . . . .......... 214
Thickness . . . . . . . . . . . . . . . . ...... 214
Mineral contents. . . . . . . . . . . . . . . . . 214
Organic remains • * * * * * * * * * * * * * * * * 215
Remarks preliminary to the following
rocks and groups . . . . . . . . . . . . . 217
26, GENESEE SLATE. . . . . . . . . . . . . . . . . 210
General characters, extent, etc. ...... 218
Concretions. . . . . . . . . . . . . . . . . . . . . 220
Localities. . . . . . . . . . . . . . . . . . . . . . . 220
Thickness . . . . . . . . . . . . . . . . . . . . . . 221
Minerals . . . . . . . . . . . . . . . . . . . . . . . 221
Organic remains. . . . . . . . . . . . . . . . . 221
27. PortAGE or NUNDA GRoup ...... 224
General character and extent........ 224
Subdivisions. . . . . . . . . . . . . . . . . . . . . 226
1. Cashaqua shale. . . . . . . . . . . . . . . . 226
2. Gardeau shale and flagstones. . . . . 227
3. Portage Sandstones . . . . . . . . . . . . . 228
Diagonal lamination . . . . . . . . . . . . . . 230
Ripple marks. . . . . . . . . . . . . . . . . . . . 230
Casts of shrinkage cracks . . . . . . . . . . 230
Concretions . . . . . . . . . . . . . . . . . . . . . 230
Casts of flowing mud . . . . . . . . . .... 332
Casts of mud furrows and striae..... 234
Localities. . . . . . . . . . . . . . . . . . . . . . . 287
Thickness . . . . . . . . . . . . . . . . . . . . . . 238
Minerals . . . . . . . . . . . . . . . . . . . . . . . 239
Springs........................ 233
Agricultural characters. . . . . . . . . . . . 239
Organic remains . . . . . • . . . . . . . . . . . 241
Localities of superposition. . . . . . . . . . 248
Ithaca group. . . . . . . . . . . . . . . . . . . . . . . 250
28, CHEMUNG GROUP . . . . . . . . . . . . . . . 251
General characters and subdivisions... 251
Diagonal lamination and structure of
strata . . . . . . . . . . . . . . . . . . . . . . 256
Concretions . . . . . . . . • . . . . . . . . . . . . 257
Spheroidal desquamation........... 257
Ripple marks. . . . . . . . . . . . . . . . . . . . 257
Localities. . . . . • . . . . . . . . . . . . . . . . . 258
Thickness . . . . . . . . . . . . . . . . . . . . . . 260
Mineral contents . . . . . . . . . . . . . . . . . 260
Springs . . . . . . . . . . . . . . . . . . . . . . . . 260
Agricultural characters............ 260
Organic remains . . . . . . . . . . . . . . . . . 261
Localities of Superposition ......... 276
XIV CONTENTS,
CHAPTER WI.
OLD RED SANDSTONE.
Relative position, extent, etc . . . . tº gº e a tº e º e º e º e º e º & Q & 6 tº . . . . . . . . . . . . . . . . . . . . . . . . 278
Localities . . . . . . . . • . . . . . . . . . . . e tº e º gº tº a • * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * 280
Organic remains. . . . . . . . . . . . . g e e º C tº a 0 e º e º e 6 © C & © & © 0 & 0 & O C C C C C C C C C C Q tº e º O & © tº º 0. 280
CHAPTER WII.
CARBONIFEROUS SYSTEM.
Conglomerate or equivalent of the millstone grit of England. . . . . . . . . . . . . . . . . . . . . . 284
Diagonal lamination . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 286
Concretions . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 287
Localities . . . . . . . . . . . . . . . . . . . . . . . tº º e º O & & © 4 & © & O & 0 & 0 & © e º O © tº e o gº e º 'º e º e º e g tº ... 289
Thickness. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 291
Organic remains . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 291
CHAPTER VIII.
Uplifts, dislocations and undulations of the strata in the Fourth District. . . . . . . . . . . . . . . . . . . . . . 295
CHAPTER IX.
Jointed structure of the rocks of the Fourth District. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 299
Jointed structure of the limestones. . . . . . . . . . . . . . . • . . . . . . . . . . . tº C & G & º ºx & © tº e & . . . . . 302
Jointed structure of the shales and sandstones . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 303
Jointed structure of conglomerate. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 307
CHAPTER X.
Mineral and gas springs, rising from the rocks of the New-York System in the Fourth District, 308
1. Nitrogen springs . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 308
2. Springs evolving carburetted hydrogen and petroleum (Burning springs), . . . . . . . . . 309
3. Sulphuretted hydrogen springs. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 311
4. Salines or brine springs . . . . . . . . . . . . . . . . . tº e º e º 'º e tº gº © tº e s ſº tº e º & © ſº º e º º gº tº º & © tº e e 314
Tabular list of the Mineral Springs in the Fourth District, with their Geological position
and products. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 315
CHAPTER XI.
NEw RED SANDSTONE AND TERTIARY . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 317
CONTENTS, XV
CHAPTER XII.
SUPERFICIAL DETRITUS • * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * e e 3.18
CHAPTER XIII.
Position and mode of transport of the great northern boulders. . . . . . . . . . . . . • - - - - - - - - - - . . . . 332
CHAPTER XIV.
Modern superficial deposits. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 842
CHAPTER XV.
LAKE RIDGES.
Ridge road of Lake Ontario and Lake Erie. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ... 348
Terraced hills. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 352
Modern lake ridges and beaches. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .354
CHAPTER XVI.
Muck Swamps. . . . . e e º 'º e º e º e º e º e e e e e s & e tº e e e e s e e e º 9 e e º e e º e º 'º e o e º e o e o e s e o e e 359
Lake marl and tufa or Travertine. . . . . . . . . . . . . . . © e º e º e º e to e º e º Q tº e º e º e e g o e o º e º e 360
Discoloration of Sands and clays by percolating water . . . . . . . . . . . . . . . . . . . . . . . . . . . . 361
CHAPTER XVII.
Fossil bones of quadrupeds. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 362
CHAPTER XVIII.
Modern action of rivers; Freezing of water in river channels . . . . . . . . . . . . . . . . . . . . . 368 .
CHAPTER XIX.
Waterfalls. ... . . . . . . . . . . e C tº 0 = * * * > 0 e º 8 e e º e º e º O © e º O e º 'º e º e º e º e º e º e º e º e º 'º e a e º e 377
CHAPTER XX.
Niagara Falls, its past, present, and prospective condition, . . . . . . . . . . . . . . .......... 888
Trigonometrical survey and map of Niagara Falls . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 402
XVI CONTENTS.
CHAPTER XXI.
LAKES,
Lakes of the district, their geological situation, etc. . . .
© e º e º 'º & O © e º e º ºs º e º e º e º e º 'º e º c 405
Elevation and depression of water in the great lakes. . . . . . . . . . . . . . . . . . . . . . . . . . . . 408
Mean length, breadth, elevation and area of the several great lakes
Elevation of the smaller lakes. . . . . . . . . . .
Elevation of different points in the district, from Lake Ontario Southward ...
CHAPTER XXII.
to e º º e º e º e º e º e º e º e e 411
e e e º e o e º e º 'º e º 'º e º 'º e e Q & e e 412
. . . . . . . . 413
Local geology and economical products of the counties comprising the Fourth Geological District, 414
Wayne county . . . . . . . . . . . . . . . . . . . . . . .
© º Q e Q & Q e º e tº e e º e º e 0 e º e º 0 o 0 414
Monroe county . . . . . . . . . . . . . . . . . . . . © º 0 & 0 & 0 & © e º O © Q & Q & Q & Q @ º O e º 'º e º e º O e e 422
Orleans county . . . . . . . . . . . . . e e e tº e º e C © tº e º e e
Niagara county. . . . . . . . . . . . © e º e º e º O O e º 0 e º 0.
Seneca county . . . . . . . . . . . . . . . . . . . . . . .
e e e e º e º e º e e º 'º e º e o e º e e Q e º 'º e e 433
© e e º O e º O e º e º e º e º O O e º O & C & e o 0 440
e e e º e º e º e º e º e º e e º e e o e o e e- g º e º te e º Q 449
Ontario county 0 e º 6 e º a 0 e º O 9 @ e º 'º e º O ſº e º O C C C C & Q e e º 0 ° tº e o e º O O. c 0 , e. e º 0 & 0 e tº gº tº 453
Yates county. . . . . . . . . . . . . . . . . . . .
© e º Q & © º ºs º e º e º G & © Q
e º e º C & © tº e º e º e º e º e º 'º º 458
Livingston county................ • * * * * * * * e Q e º 0 e º O C e º O O 9 e º e º e º e º e o 6 e e Q 9 459
Genesee county. . . . . . . . . . . . e e º e º e º e Q Q - e. e º ſº tº
Erie county . . . . . . . . . . . . . . . . . . .
Chemung county . . . . . . . . . . . . . . . . . . . . . . . . . .
Steuben county. . . . . © e º 'º e º 'º e e º 'º e e e º e º Gº © e e º º
Allegany county . . . . . . . . . . . .
Cattaraugus county. . . . . . . . . . .
Chautauque county . . . . . . .
CHAPTER XXIII.
e Q e º e º 'º - e. e. e. e º 'º e º 'o e º 0 e o ºs e e º e º e º e
e e º O e º e Q © e º 'º e e e º e º e º e º a e º e O 464
• e º e º 'º e e º e º e o e s e º e º e º e e e º 0 e º 0 e o e e º 'º e º 0 469
Tompkins county (western half) . . . . . . . . . . . . © e º 'º e º ſº tº e º & © e º 'º e º e º O Q
. . . . . . 475
• e e º e o a c e e e o e o 'o e a e º e e o e o e 9 477
e & e º e º e o e º e º e º e º e º e e e º e º 'º 6 tº 480
& © e º e º e e º 0 484
• - - - - - - - - - - - - - - - - - - - - - - - - - - - 488
• . . . . . . . . . . . . . . . . • e e s e e o e º e o s a e s e o e e o e s e e s e e 493
On the identity of the rock formations of the western States with those of New-York.......... 500
CHAPTER XXIV.
On the identity of New-York formations with those of Europe.
Caſl Strata. tº e º e º 'º º e º 'º e º 'º e º O tº e º e º 'º
CHAPTER XXV.
CONCLUSION.
• e o e e s a e e o e o a e e º e e
Table of Equivalents in Ameri-
© tº t e º 'º e º 'o e e º e e. e. e. e. e. e. e. e. e. e. e º a tº 516
LIST OF IL LUSTRATIONS,
No. Page.
1. Section, illustrating the order of succession of the strata in New-York. . . . . . . . . . . 27
2. View of Medina falls . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 34
3. Diagonal and curved lamination of strata . . . . . . . . . . e 9 & 0 & 0 & 0 e º & © tº e º 'º e e e º e < e e 40
4. Ditto . . . . . . . . . . e e º e º 'º e º 'º e º e º e • e º e º e º 0. e e e º e e º 0 to e º 0 & © e º 'º e a e 41
5. Fossils of Medina sandstone,. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 46
6, T)itto e e º e º e e º e o e e 2 e e a e º e º e º e G e tº e º e º e ºs e e º e º e º 'º © e º e º O & © e º 'º e 48
7. Ripple marks. . . . . . . . . & © º e º e e Q © º e Q & © tº e e e º e º 'º e º O e º 'º e º 'º t e º 'º • . . . . . . . . . . . . 49
8. Surface of stratum of the Medina Sandstone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 50
9. Shrinkage cracks of the Medina sandstone. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 51
10. Stranded shells with ridges of sand.............. tº e º e º O e * @ Kº e º e º 'º tº º O ſº e ºs . . . . . 52
11. Wave lines . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . • . . . . . . . . . . . . . . . . . . . 54
12 and 13. Modern illustrations of the two preceding cuts . . . . . . . . . . . . . . . . . . . . . . . . 56
14, Fucoids of the Clinton group . . . . . . . . . . . . . . . . . . . . . . . . . . . . & tº e º 'º e e Q • . . . . . . . 69
15. Fossils of the Clinton group . . . . . * e º e º e º e • . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 70
. 16. T)itto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 71
17. Ditto . . . . . © e e g tº e º 'o e º e 9 ſº e º e º 'º e º e º 6 tº e º e º e º e g º e a c e e º e Q & gº tº e º e C 72
18. Ditto tº e º e º a G e º e º a tº e º e º e º sº e C & © • . . . . . . . . . . . . . . . . . . . . . . . . . . . . 76
19. Ditto . . . . . . . . . . . . tº e º e º e º e e Q @ e º 'º e º e º 'º e º e º e e © e º O e e º 'º . . . . . . . . 77
20. Section illustrating the order of succession. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 78
21. Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 79,
22, View of Niagara falls. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 80
23. Upper falls at Rochester . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 82
24, Concretionary and contorted strata . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 86
25. Porites, cavity formed by the removal of . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 86
26, Fragments of encrimital columns . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 90
4*
XVIII LIST OF HILUSTRATIONS.
27. Porites with linear cavities from the removal of crystals. . . . . . . . . . . . . . . . . . . . . . . 91
28. Undulation and thickening of strata. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 92
29. Concretionary structure in Niagara limestone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 93
30. Curved or concretionary strata—View of Porter's quarry, Niagara falls. . . . . . . . . 94.
31. Similar structure to the above, from the Third district. . . . . . . . . . . . . . . . . . . . . . . . . 94
32. Lignilites, or Magnesian stria . . . . . . . . . . . . . . . . . . . . . . . .................... 95
33. Fossils of the Niagara group . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 101
34. Ditto ... . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ................ 103
35. Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 104
36. Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 105
37 and 38. Ditto e e a e e º e o 'º e º e o e e º e o e º e e s a G e º e º 'º e º O © e º 'o e º 'º e o e º s
39. T)itto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 109
40. Ditto • . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 110
41. T)itto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 112
41 (read 41 bis). Ditto ................................ . . . . . . . . . . . . . . . . . . . . 113
42. Ditto .................................................... 115
43. Titto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 116
44. Section illustrating the order among the strata forming the Onondaga Salt group.... 119
45. Section of a gypsum quarry . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 121
46. Section on the bank of the Canandaigua outlet; gypsum quarries. . . . . . . . . . . . . . . 122
47 and 48. Gypsum quarries. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 123
49. Ditto • - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - . . . . . . 125
50. Pseudomorphous hopper-shaped crystals . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 127
51. Porous or vermicular limestone. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 128
52. Lignilites, or epsomites . . . . . . . . . . . . . . . . . . . . . . . . . . . • . . . . . . . . . . . . . . . . . 130
53. Vertical suture of the same . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ........ 131
54. Fossils of the Onondaga salt group . . . . . . . . . . . . . . . . . . . . . . . . . . . ............ 137
55 and 56. Sections showing the order of superposition. . . . . . . . . . . . . . . . . . . . . . . ... 139
57. Water-limestone with linear cavities. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 142
58. Fossils of the Water-lime group . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 142
59. Fossils of the Oriskany sandstone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ........ 148
60. Ditto . . . . . . . . . . . e e e e e º e a e º e º 'º º 'º e º e º e * * * * * * * * * e. e. e. e. e. e. e. e. e. e. e. e. 149
61. Fossils of the Onondaga limestone. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 157
62, Ditto • - - - - - - - - - - - - - - - - - - - - - . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 159
63. Ditto G e º 'º e º Q o e º e º e . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ...... 160
64. View of a quarry in the Corniferous limestone. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 161
65. Sections showing supposed faults of strata in the Corniferous limestone... . . . . . . . . 163
66. Sections showing fissures in the Corniferous limestone . . . . . . . . . . . . . . . . . . . . . . . . . 169
67. Fossils of the Corniferous limestone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 171
68. T)ilto e & tº G º 'º e º e º e º 'º e º e • - - - - - - - - - - - - - - - - - - - - - - - - - - . . . . . . . . . 172
69. Ichthyodorulite. . . . . . . . . . . . . . . . . . . . . . . . • - - - - - - - - - - - - - - - - - - - - - - - . . . . . . . . 174
70. Fossils of the Corniferous limestone.................. .................... 175
71, Fossils of the Marcellus shale . . . . . . . . .
• * * * * * * * * * * * * * * * * * * * * * * * * * * * * * a • a e 180
LIST . OF ILLUSTRATIONS.
XIX.
72.
73.
74.
75.
76.
77.
78.
79.
80.
81.
82.
83.
84.
85.
86.
87.
Section on the outlet of Conesus lake, one mile west of West-Avon, Livingston co.
Section of the bed and bank of Allen's creek, at Le Roy village . . . . . . . . . . . . . . .
Jointed structure of the cliffs on Cayuga lake . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Concretion enclosing a fossil. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . tº s e º e e s e
Septaria tº e o e º e º e o e º e º e º e º 'º e º 'º e e º 'º e º e º e º e a tº º e º e º e º 'º - e º C º e º e º e e º 'º e 6, 9 @ e e
Fossils of the Hamilton group . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto e e º e o e s e s e e o e º 'º e o e º e º e s e e s e º e s e • * * * * * * * * * * * * * * * * * * *
Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto • - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - • * * * * * * * * * c e o e e e e e s e
Ditto • * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * *
Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto s' s e º 6 e e º e º e º 'o e ºs e º 'º e º t e s e º e s e e º e-e e o e e º e a e e s e e a e e s e e o e
Ditto ... . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ........
Ditto . . . . . . . . e e e º e º e º e º 'º e º 'º e º e º e º e º e º 'º e s a s e a e e a e e e e e e º e e e
Ditto • - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
88 and 89. Sections illustrating superposition of strata............................
90.
91.
92.
93.
$94,
95.
96.
97.
98.
99.
100.
101.
102.
103.
104.
105.
106.
107.
H08.
109.
110.
111.
112.
113.
114.
115,
Tully limestone—Sketch on Seneca lake . . . . . . . . . . . • - - - - - e '• • - - - - - - - - - - - -
Curve in the Tully limestone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Fossils of the Tully limestone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Fossils of the Genesee slate ............ . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto • e e s e s e e s a e e e s e s a t e s e e e s e e s - e o e • e º e e º e s e e s e e s e e º e e e e
View of Upper and Middle falls, Portage ............................. © e e º e
Section showing subdivisions of the Portage group . . . . . . . . . . . . . . . . . . . . . . . . . .
View on Cashaqua creek . . . . . . . . . . . . . . . . . . ............................
Septaria, from Portage group. . . . . . . . . . . . • . . . . . . . . . . . . . . . ------ . . . . . . . . . .
Cone in cone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . © tº e º e º e º e e • • - - - - - - -
Cast of flowing mud . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Cast of striae . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Cast of mud-furrow with shells . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Fossils of the Portage group . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto e e o e o e a e º 'º e o e o a c e º e º 'º e º º e o e o e º e o e a e - e. e. e. e o 'º e e o 'o e º 'º e º e &
Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto ... . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto * - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
View on Cashaqua Creek. . . . . . . . . . . . . . . . . . . . • - - - - - - - - - - - - - - - - - - - - - - - - - - -
Fallcreek, near Ithaca. ................................................
Chemung Upper narrows. . . . . . . . . . . . . . . . . . . . . . c e e e º 'º e º 'º e º e a e e © º ºs e º 'º o e =
Section showing the Succession in the higher groups. . . . . . . . . . . . . . . . . . . . . . . . . .
Concretionary structure of strata .........................................
Ripple-marked surface. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Section of cliff showing ripple-marked strata. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
133
183 .
184”
192
193
193
196
198
200
202
203
204
205
207
208
209.
211
212
214
215
216
222
223
224
226
226
231
232
233
235
237
241
242
243
245
247
249
250
251
253
257
258
258
XX
LIST OF ILLUSTRATIONs.
116 and 117. Fossils of the Chemung group. . . . . . . . . . . . . . . . . . . e e e º C G e º e e e º O & © &
1 18.
119.
120.
121.
122.
123.
124.
125.
126.
127.
128,
129.
130.
131.
132.
133.
134.
135.
136.
137.
138.
139.
140.
141.
142,
143.
144.
145,
146.
147.
Ditto • . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . • * * * * * * * * * *
Ditto • . . . * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * * *
Ditto • a e e º e e e e e s e e e e o e º 'º e e s e e e a e e e o e º e º e º 'º e º e
Ditto G s e º e e e º e º O e º e º e e º 'º © e e º e º e e º e º e º 'º º e Q & © tº e º &
Ditto © e º ºs e º e º Q & e º º e e e º e º e e º 'º - e º O © e Q tº e e º e e . . . . . .
Ditto - 9 s e e º e º e º O © tº Q e 6 e tº e º e º e a c e o 0 ° º e º O e º 0 ° º e º O & © tº
Ditto * c e e º e s e a • e o e s e e e e º 'º e º e º e º ſº e e e º 'º e º e o e º e º O & © tº
Ditto • e e e e e o e e e s e e e e º e e o 'º e e o e º e e o 'º e º 'º e º 'º e º e º 'º e º e
262
263
264
. . 266
267
269
270
271
273
Section at Sexton's quarry . . . . . . . e e e a b º e º e s e s tº e s e e e e º e º e º e s e o e º 'º º tº e º O & © 274
Land plants of Chemung group. . . . . . . . .
Section showing the position of the Old red
Comparative section in Indiana . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .• - - - - - - - -
Fossils of the Old red sandstone........ . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Ditto - ................................. • * * * * * * * * * * * * * * * * * *
View of the outcropping edge of the conglomerate. . . . . . . . . . . . . . . . . . . . . . . . . .
Diagonal lamination in sandstone........ . . . . . . . . . . . . . . . . • * > . . . . . . . . . . . . .
Diagonal lamination in conglomerate . . . . . . . . . . . . . . . . . . . . . e e e o 'º e º 'o e º 'º & tº e º ºs
tº e > e e º e º a c e º e º e a e º º e e º º e º O & © tº º
sandstone . . . . . . . . . . . . . . . . . . . . . .
Concretionary laminae of iron ore... . . . . . . . . . e e º O e º e tº e º e º e º e o t e º 0. © g º e º G & ©
Ditto . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Similar concentric laminae in the conglomerate and Sandstone of Ohio . . . . . . O e º O
View in Rock city, Cataraugus county...................................
Fossils of the conglomerate ............... ............................
© º e º e Q
Section showing the position of the conglomerate at Cuyahoga falls, Ohio . …
Uplift near Eighteen-mile creek, Lake Erie . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Uplift, Ripley, Lake Erie shore........................................
Uplift, South branch of Cattaraugus creek . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Uplift at Little's mill, South branch of Cattaraugus creek . . . . . . . . . . . . tº e º ºs e º e e
View of the cliffs on Fall creek . . . . . e e º 'º e º 'º e º º e º & © º G • * * * * * * * * * * © e º e g º º e e
Joints in shaly strata, Twenty-mile creek . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Joints in limestone....................................................
148. Jointed structure of cliffs on Seneca Lake and at Lodi .......................
149.
Jointed structure of cliffs on Cayuga lake............................. vº º e
150 and 151. Jointed structure of cliffs on Seneca lake...........................
152 and 153. Ditto • - - - - - - - - - - - - - - - - - - - - - - - - - ‘............ © e º 'º
154.
155.
I56 and 157. Sections illustrating the geological position of
158,
159.
160.
161,
Jointed structure of the conglomerate. . . . . . . . . . . . . . . . . . . . . . . . . . . . . .......
Situation of the Petroleum spring in Freedom . . . . . . . . . . . . . . . . . . . . . © e º 'º e º e tº
springs. . . . . © e º ſº e º 'º C tº e º e º ſº e e Q & © tº e º e © º e º 'º & © e º e º e © C & 0 & 0 e o e º e &
Section of drift at Vinton's quarry, Lake Ontario . . . . . . . . . . . . . . . . . © tº e º O © e e s e
Section of drift at Wilson, Niagara county ... . . . . . . . * @ e º e º 'º e º e º e º e º e o e o 'º e
Section of drift near Rochester tº º e º O & ſº e o 'º e • * * * g e a e º º e º 'º e s e o e º e º e e e º e e s a e
Grooved and polished limestone, Lockport ................................
the sulphureited hydrogen
275
278
280
281
282
284
286
287
287
288
288
290
291
292
295
296
297
298
299
300
303
304
. 304
305
306
307
310
314
322
323
324
326
LIST OF ILLUSTRATIONS.
XXI
162. Position of the grooved limestone in the Clinton group, near Lewiston. . . . . . . . . .
163. Section of drift and more modern deposit ... . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
164. Section of drift on Lake Ontario ... . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
165. Weathered mass of hydraulic limestone...................................
166. Alluvial hills and terraces. . . . . . Q & e º e º e e s e e s s • e • e e is e º e s e s • e s e s - e s = • * * * * *
167. Section of modern detritus at Portage . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
168. Ridge road, division of ...............................................
169. Terraced hill, Jefferson. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
170. Map of small ponds on Lake Ontario . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ...
171. Sandbar at outlet of Stream . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . tº e e &
172. Discoloration of clay by percolating water . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
173. Tooth of Mastodon . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
174. Lower falls of Portage . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .........
175. Section at Portage. . . . . . . . © dº e º e º e o e o e º C º e º e º dº º • * * * * * * * * * * ,
176. Plan of river at Portage . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ........
177. Transverse section of the Genesee at Portage......................
178. Course of the Genesee river below Portage. . . . . . . . . . . . . . . . . . . . . . . .
179. Entrance of Wolf creek into the Genesee river............................
180. Elevation of strata by freezing water ........ • * * * * * * * * * * * * * * © º º e º e o e º e e ©
181. Taghanmuc falls, Tompkins county. . . . . . . . . . . . . . . . . . . . . . . . . . . . . &
182. Hector falls, Tompkins County . . . . . . . . . . . © º e º e º e o a c e o e e Q & © a e e o e o e s a e e a
183. Falls on the Canaserowlie creek, Cattaraugus county.......................
184. Section of rocks on the Genesee, below Rochester . . . . . . . . . .
185. Lower falls of the Genesee, Rochester ...... & © tº e º e º 'o e o e º e º e * * * > 0 e o e º e e e e e
186. Section along the Niagara river . . . . . . . . . . . . . . . . . . . . tº e º e º 'º º 6 e º e s e e o e º e º e
187. Transverse section of the Niagara river . . . . . . . . . . . . . . . . . . . . .............
188. Section along the Oak-orchard creek . . . . . . . . . © e º a c e o e e e s e e e s e e e a e e
189. Transverse section of Niagara at the falls...... * * * * * * * * * * * * e o e a • e e s e
190. Conesus lake . . . . . . . . . . . . . . . . . . . . . * * * * * * * * * * * * * * e o e e o e s e e e e e e e s e a e s a
191. Drift hills, Lockport . . . . . . . . . . . . . . . . . . . . . . . . . . . . . & ſº 0 tº 0 e º O O & ©
192. Section of strata at Lewiston, showing a depression filled with fragments from above
& © tº e º c e e
LITHOGRAPHIC PLATES.
329
339
340
341
342
345
. 350
352
. 355
356
362
363
368
369
370
372
. 373
374
. 375
377
379
. 380
. . . 381
382
383
. 391
393
. 397
405
. . 440
441
Birdseye view of Niagara falls and river . . . . . . . . . . . . . . • . . . . . . . . . . . . . . . . . . . . . 383
View of Niagara falls, by Hennepin. . . . . . . . . . . to @ Q Q & O © tº e e º ºs . . . . . . 395
Trigonometrical map of Niagara falls. . . . . . . . . . . . . . . . .................. © Q 404
TABLES OF FOSSILS USED IN THE DESCRIPTIVE PART OF THIS WORK,
Numbered at the bottom from 1 to 66.
XXII
LIST OF ILLUSTRATIONS.
:
13.
14.
15.
16.
17.
18.
19.
. Organic remains of the Medina sandstone.
. Surface of Medina sandstone, with current marks,
. Fin and scales of Sawripteris Taylori. Old red sandstone.
. Natural section of Niagara river. (Colored.)
LITHOGRAPHIC PLATES AT THE END OF THE WORK.
6, 6, a and 6 b. Coast section of lake from Black-Rock to the Pennsylvania line.
. Section across the formations between Lake Ontario and the northeastern extremity of the
Pennsylvania coal field. (Colored.)
. Uplifted strata and intermingled drift. (Colored.)
10, 11 and 12. Section across the several counties of the Fourth district. (Colored.)
Natural section of the Genesee river from Mount-Morris to Portage, New-York; and one
from Cleveland, Ohio, to the Mississippi river. (Colored.)
Grooved and striated surface of limestone, with projecting knobs of hornstone,
View from Big-flats, Chemung county.
Ravine at Hammondsport, Steuben county.
Hector falls, Tompkins county.
Lodi falls, Seneca county.
Deep gorge of the Genesee at Portage.
GEOL06;ICAL MAP OF NEW-YORK,
The accompanying Geological Map of the State is intended to present a clear idea of the general
geological divisions which have been enumerated in the reports. In a few cases it has been found im-
practicable, from the small scale of the map, to indicate all the subdivisions. Thus the lower limestones
(Birdseye and Trenton) are blended in one color. The same course has been adopted in relation to the
Helderberg division, where the small extent of surface occupied by each member would preclude the
indication by separate colors. There is no difference in color to indicate the line of demarkation between
the Portage and Chemung groups, and in truth there is no distinct line of separation in lithological cha-
racters between the two. All cases of decided change in lithological character are indicated by color.
That part of the map appertaining to the Fourth district presents a series of almost parallel lines of
color, showing the limits and the undisturbed range of each formation, rising one above the other on
the South in a series of steps or terraces.
The tabular arrangement of colors in the margin, will indicate the formation marked by any par-
ticular color upon the map. The transverse sections at the bottom of the map, colored in the same
manner, illustrate very satisfactorily the order in which the strata naturally overlie each other. From
these alone, the map will be understood without consulting any other explanations, except in cases where
there is disturbance or derangement of the strata.
The Carboniferous strata within the State are only in isolated patches, consisting of the conglo-
merate and associated sandstone. In some of the maps, a portion of the State of Pennsylvania has been
colored under the direction of Prof. H. D. Rogers, and this illustrates more clearly the connexion
between the rocks of New-York and the coal-bearing strata of Pennsylvania.
The coloring is continued beyond the Niagara river, showing the undisturbed continuation of the
rocks of the Fourth district into Canada.
5*
EXPLANATION OF THE DIAGRAM.
§
jo
|
-**
:
§
;
§
3.
*
3
S
:
sº
s:
*3
A. Entrance to the room.
B. B. Stairs to gallery.
CCCCCCCC. Windows.
D. Table.
EEEEEEEEE. Vertical cases standing against the
side of the room.
The figures indicate the Tabular cases, with the -
| contents, as follows:
1. Primary system.
2, Taconic (Taghcomick) system.
NEW-YORK SYSTEM.
3–1* Potsdam sandstone.
4–2
. Calciferous sandrock.
. Black-river and Birdseye limestone.
. Trenton limestone.
. Utica slate.
8–6. Hudson-river group.
10–8
. Grey sandstone.
. Oneida conglomerate.
11–9. Medina sandstone.
12–10.
13–11.
14–12.
15–13.
16–14.
17–15.
18–16.
19-17.
20–18.
21–19.
22–20.
23–21.
24–22.
25–22.
26–23.
27–24.
28–25.
29–26.
30–27.
31–28.
Clintom group.
Niagara group.
Onondaga-salt group.
Waterlime group.
Pentamerus limestone.
Delthyris shaly limestone.f
Oriskany sandstone.
Cauda-galli grit.
Schoharie grit.
Onondaga limestone.
\ tº - º
Corniferous limestone.
Marcellus shale.
Hamilton group.
Hamilton group.f
Tully limestone.
Genesee slate.
Portage group.
Ithaca group.
Chemung group.
Catskill group or Old Redsandstone.
CARBONIFEROUS SYSTEM.
*
&T II 0T
# {{
GO
32. Conglomerate.
33. Coal and coal plants from Pennsylvania."
34. Red sandstone and associated trap rocks of
Southern New-York.
35. Boulders.
36, Sands and clays.
37. Marl and modern tertiary fossils.
ºk The second series of numbers are those attach-
ed to the cases in the room, showing the succession
among the rocks of the New-York system.
+ The Encrinal and Upper Pentamerus limestone,
are not separated in the arrangement.
# Two cases are occupied by the Hamilton group.
s The New-York series ends with the Conglome-
rate, and these specimens from the coal fields of
Pennsylvania are introduced for the purpose of
showing the relative situation of those rocks.
PLAN OF ARRANGEMENT
IN THE
STATE G E 0 L () GIC A. L () 0 L L E GTI () N.
The plan of arrangement adopted in the State Collection has been, as far as possible, in the order of
nature. The object to be attained, being the dissemination of information among a large number of
persons who have given little attention to the science of Geology, the simplest mode of presenting the
subject would of course be most satisfactory. The room appropriated for the purpose is about seventy
feet long and thirty-four feet wide. Around the outside of this room is a series of vertical cases, and
about four feet within this area is a series of tabular cases; thus presenting a double series of specimens.
A single case is devoted to the productions of a rock or group, and nothing foreign to it is allowed to
enter. Each tablular case, being 3% feet long by 2; wide, contains from 50 to 70 typical specimens of
rocks and fossils of the group, giving the observer at a glance a comprehensive view of the most pro-
minent and important features of each. In the vertical cases a more numerous collection is arranged,
and the more rare or less characteristic productions of the rock or group here find a place.
The accompanying diagram will render this description more intelligible. On entering at the door,
the visitor turns to the left, bringing himself in front of the range of vertical and tabular cases, (reference at
present being had to the latter only.) The first case presents him with the most characteristic and impor-
tant varieties of granite, gneiss and associated rocks and minerals. The second presents a series of
magnesian slates, crystalline limestones, etc. being a metamorphosed group known as the Taconic (Tagh-
konic) system. The third case presents the products of the lowest known sedimentary rock containing
organic remains—the Potsdam Sandstone. From this point every successive case at the right hand pre-
sents the observer with the next rock in the ascending order of the series; and by passing on in this
direction around the room, the whole series is examined in their natural order of superposition.
By the aid of sections this is made intelligible even to the least initiated, and has proved a very satis.
factory mode of arrangement. The series terminates in New-York with the conglomerate of the Car-
boniferous system, and the next case is devoted to a collection of coal and coal plants from Pennsylvania,
showing the full development of the group. Succeeding this we have the red sandstone of the southern
part of New-York, being the New red, or of a formation intermediate between it and the coal. The three
remaining cases are devoted to surface products, as boulders, sands and clays, marl, peat, and modern
tertiary fossils. *gº
The collection of fossils, not yet completed, is to be arranged in drawers beneath these cases. In the
gallery of this room there is a geographical collection of specimens, presenting the productions of each
county separately arranged.
REPORT
OF THE
SURWEY OF THE FOURTH GEOI,00ICAL DISTRICT,
CHAPTER. I.
PRELIMINARY CONSIDERATIONs.
THE Fourth District comprises fifteen and a half counties, as previously enumerated; and
embraces all that part of the State lying west of the parallel of Cayuga lake, and included
between the Pennsylvania line on the south and Lake Ontario on the north.
The succession of strata, occupying the different portions of this district, have been made
known from time to time, in the several Annual Reports presented to the Legislature. It
now remains to give a connected view of these, with their striking features and fossil contents;
the object of the work being to aid those who wish to obtain a knowledge of our rocks, and
also to show as far as possible, by an exhibition of their distinctive features, the reasons on
which the subdivisions have been founded. With this design, some wood-cut illustrations are
given of characteristic scenery, when the rocky strata are exhibited. The principal illustra-
tions, however, are those on which the geologist depends when making his explorations in
the field — the organic contents of the rock. Wood-cuts of the most important and charac-
teristic fossils of each rock and group are inserted in the text, under the proper heads. Thus
each rock will be represented in its most characteristic fossils, which will greatly aid the stu-
dent who has not the advantage of an arranged collection for reference, and enable him to
decide from a few specimens the situation of the mass he is examining. This mode was
adopted, believing it would be impossible to present a satisfactory report without such illus-
trations.
GEoL. 4TH DIST. 1
2 GEOLOGY OF THE FOURTH DISTRICT.
The great object of the survey, as originally contemplated, was to lay before the people of
the State as much practical or available information as possible, in regard to the rocks, mine-
rals and soils. These, then, were the prominent points to be kept in view. In attempting to
do this, the manner and matter are not always such as would have been chosen, had the
report been a communication to a body of scientific men. On the other hand, it is impossible
to avoid the use of terms, some of which are strictly technical, and others not familiar to
every reader. Still many of these terms are being introduced into our English dictionaries,
and will soon be considered a part of the language. Those which are not thus used, are
readily found and clearly defined in the Glossary; and as every term employed is more ex-
pressive or significant of the idea, than words of ordinary language, it is presumed that the
knowledge of such, and their application, will fully repay every one the trouble of adding
them to his vocabulary.
Were it possible to use the familiar language of conversation so as to give names to all the
objects, and to describe all the phenomena of nature, it would perhaps be desirable to do so;
but as our knowledge of nature increases, our vocabulary becomes deficient, and we are com-
pelled to resort to other languages for terms expressive of the object or idea. These at length,
and by frequent repetition, become a part of our own tongue; and in time, by familiar use,
their origin is forgotten. Thus has it been with all words and phrases introduced from other
languages. *
Now inasmuch as Natural History, in all its departments, must become a popular study,
it is evident, either that these terms must be acquired, or others substituted ; and it will
require far more labor to find familiar terms expressing the same thing, than to learn those
already applied. There is also a necessity for a universal language; for nature is universal,
and every where the same. Whatever mode, therefore, will render a knowledge of nature
of more easy acquisition to the greater number, it is the duty, as it should be the pleasure,
of every lover of nature to adopt.
In all cases, in this report, where the name of a fossil is rendered more familiar by being
translated, it will be done ; but in many instances, the name thus translated would be inap-
plicable or inconvenient. Such instances sometimes occur where fossils have been named
from theoretical considerations, which have afterwards been overturned by the acquisition of
new facts. An example may be cited in the name primigeneus or first-created, which we
cannot with propriety affirm of any fossil at the present time; as it may happen that one of
the same genus will be found in an older rock. Names expressing any quality in a superla-
tive degree are likewise objectionable, as has often been found; for so long as any remain
unknown, we cannot with propriety use the superlative signification, as it may be superseded
by the same quality in a greater degree in another individual.
Numerous objections, in popular regard, may doubtless be made to our present nomencla-
ture, but it is far easier to make objections than to propose a more acceptable substitute, and
a report like the present is not the place for reformations in science. Reform should be made
by those best acquainted with the subject; and in these pursuits, such men are usually too
PRELIMINARY CONSIDERATIONS. 3
much occupied and interested with their discoveries, to attempt innovations in the nomencla-
ture. On the other hand, those who have but partial acquaintance with the philosophy of the
subject, or with the facts, are the first to propose a reformation in the vocabulary, and from
the want of this essential knowledge, fail in attaining the object, and leave it in a worse con-
dition than before.
No one who is aware that our present system of momenclature had a beginning, and that
it is an improvement upon all that preceded it, but believes likewise that another and better
system will hereafter take its place.
The arrangment by classes, orders, genera and species, is the only one which will enable
man to systematize his discoveries or results, whether in individual objects or in philosophic
truths; and the more nearly he can adopt this mode, the more nearly has he arrived at the
order of nature; and in the same proportion, the more accurate become the details, and
consequently the general results. What is here true of individuals or facts, is true in like
manner of masses; and the application of this principle in Geology is that which is bringing
the subject more strictly within the limits of the exact sciences, or the more exact of the
natural Sciences.
In geological formations, the relative place of species, genera, Orders, etc., with their
subordinates, has not yet been determined. Thus we find a single rock, and a group of rocks,
occupying the same place in the scale, or the same column in the tabular view. This at
present is matter of necessity; for there has not been time in all cases to make the minute
examinations which are required, in order to pronounce where the limit of a genus or species
should terminate ; and therefore groups, which may be either orders or genera, hold the same
place as individual rocks which are species.
In rocks, as in other classes of natural objects, it is often very easy to discover the generic
limit, clearly and undoubtedly, as in Botany the oaks; while in other cases, as in the grasses
and flowerless plants, the most minute examination is requisite to separate genera and species.
Subdivisions will one day be made in what are now termed groups of rocks, as have been
in some of the obscure families of animals and plants; and it is well to bear in mind, that a
group is composed of an assemblage of individuals, which, for want of more accurate know-
ledge, are left thus, rather than hazard a division at present. A group, then, consists of an
assemblage of individuals. A rock constitutes both the species and genus, there being no
allied one with which it could be united to form a genus of more than one species.
From these remarks, it is not to be understood that Geology is so much more obscure or
doubtful than other sciences; for subdivisions of genera and orders of plants and animals are
constantly made, for the reasons that the individuals in question differ in essential particulars
from the descriptive characters of their former associates. The same thing has yet to be
done for Geology; what now constitute groups, will be identified as consisting of several
individuals, and separated accordingly.
In this way only, man progresses in systematic knowledge; at his first investigations,
throwing together those things which bear some obvious resemblance; and in his subsequent
examinations, with increased knowledge, making more accurate and natural Subdivisions.
4 GEOLOGY OF THE FOURTH DISTRICT.
In our own geology, the first step towards this degree of perfection has been made in the
groupings adopted in the Reports. This was all that could be accomplished for the present,
when the whole subject was to be reduced from its former chaotic state, and while so much
remained to be done in its other departments. The arrangement of the whole system in
classes, orders and genera, will follow naturally, from what has been done, all the elements
being prepared.
The first object in the prosecution of this survey, has been to ascertain the existence and
extent of the different rocky masses, their lithological characters, their mineral and fossil con-
tents and other associations, and their order of succession, or the manner and order in which
one rock is preceded or followed by another. Facts of this kind were collected throughout
each mass from one extreme to the other, in many cases extending across the whole State.
In this way only could the materials be obtained for forming a System, or presenting in their
proper order and association the collections made in different parts of the State. Thus our
rocks have been arranged, and each one holding its appropriate place in the series, its extent
and its mineral productions are easily pointed out. The relation of any one mass to others
of importance is thus readily seen, and also the relative position of the whole as regards the
great Coal formation or Carboniferous system.
Among the most important facts demonstrated in the progress of this survey, Is that of the
non-existence of the great Coal formation within the limits of New-York, except its lower
member in a few detached points or outliers. This knowledge, though negative, is neverthe-
less of great value; having forever set at rest a vain expectation, which has cost an immense
expenditure in time and money. When facts of this kind are fully understood and appre-
ciated, the importance of the survey will be seen in the abandonment of all schemes of mining
for coal and the precious metals, and the consequent quiet and satisfaction ever attendant on
rightly directed enterprise.
It is thus negatively, as well as by direct and positive discoveries, that science ameliorates
the condition of mankind; turning attention from useless and visionary pursuits, and directing
it to that which yields a ready and satisfactory result for the expenditure of labor and time.
And although the promulgation of scientific truths may restrain the vagaries of minds which
delight to build the splendid air castles of suddenly acquired wealth, it will nevertheless direct
man's energies to sources where perseverance is sure to be crowned with rewards which a
morbid fancy would crave at the commencement of the enterprise. From science alone will
man learn his true interests, as regards his well-being in this world.
In a report like the present, being the result of investigations commenced after much was
already done, and where it is not always convenient to refer to the author, time and place, a
short notice of what had been previously accomplished, and what was the condition of geolo-
gical knowledge when the survey began, will show the manner in which our rocks have been
studied heretofore, and afford an explanation of the comparatively little progress that had been
made towards a correct classification of the same.
Thirty-three years have elapsed since Mr. Maclure published his “Observations on the
Geology of the United States.” To him we are indebted for the first sketch of a system,
PRELIMINARY CONSIDERATIONS. 5
and a geographical distribution of the rocks of this country. At that period, it was impossible
to give the connected and systematic information which years of experience have enabled us
to acquire; and no attempt was made, farther than to identify our strata with those of the
eastern continent.
It would be useless to follow, in chronological succession, those who have labored at the
same task, viz. not to develop the system of rocks as they are, but to identify them with
the known formations of Europe. This undertaking, as we have learned from experience,
was at that period a hopeless task; for only very recently have we obtained any thing like a
correct classification of the older deposits in England, while on the continent much yet
remains to be done. Under such circumstances, it is not surprising that many errors were
committed, and our progress in the science consequently retarded.
The name of the late STEPHEN VAN RENSSELAER will always be remembered with reve-
rence by the American student of geology, and perhaps scarcely less so in other branches of
natural science. Through his munificence, Professor EATON was enabled to make a very
extended and systematic survey of the rocks of New-York; and if, in his report, some things
are not perfectly in accordance with recent discoveries, we must remember that at that period
he was almost entirely without a guide in these older formations; that he was in fact describ-
ing rocks which at that time were not understood in Europe, and which no geologist had yet
attempted to classify. Had he evinced still more independence of European classifications—
as is now recommended from high authority on the other side of the Atlantic — pursued the
investigations of the subject to a more thorough detail; published sections illustrating the order
of Superposition from the older to the newer rocks, with their fossils so numerous and so cha-
racteristic, he would have left an undying fame to himself and his noble patron. We can
only regret that this was not done in the most extended and perfect manner, since it is evident”
that on the part of Mr. Eaton every desire existed to do so, while the means furnished by Mr.
Van Rensselaer were unlimited for illustrations of every kind; yet so trammelled was the
former by European authorities, that no more was produced than the imperfect sketch then
presented to the public.
In that work (Survey of the Canal Rocks), which was published in 1824, it is evident
that the author was fully aware of the great extent of our undisturbed strata as compared with
those of Europe. He remarks, that “Our secondary rocks along the canal line are several
“hundred miles in extent, and remarkably uniform in their leading characters.”
“After examining our rocks with as much care and accuracy as I am capable of doing, I
“venture to say, that we have at least five distinct and continuous strata, neither of which
“can with propriety take any name hitherto given and defined in any European treatise which
“has reached this country. The late work of Philips and Conybeare describes many of the
“beds, and some of the varieties found among the rocks referred to ; but the momenclature
“of these very able geologists cannot be adopted in our district, without mangling and dis-
“ torting the unprecedented simplicity of our rock strata.”f
* Canal Rocks, pages 8 and 9. f Ib. page 7.
6 - GEOLOGY OF THE FOURTH DISTRICT.
I quote this, to show that Mr. Eaton was aware that the names and arrangement adopted
in the systems of European authors did not apply to the rocks of New-York; and yet, most
fatally, he attempted to apply that arrangement as far as possible, all the time supposing him-
self to be investigating rocks of the same age, while in truth they were much older than any
described by the authors quoted. This attempt to identify the rocks of New-York with the
Secondary system of Europe, probably arose from the general belief that the older or Transi-
tion strata were in a highly disturbed and altered condition, having undergone mutations by
which nearly all the organic forms were obliterated. Thus when so great a range of undis-
turbed strata, abounding with organic remains, was presented, as along the line of the Erie
canal, it was quite natural to refer them to the secondary deposits; indeed it required know-
ledge, at that time not possessed in our country, to decide the true age and position of these
rocks. * .
In that work, nearly all the rocks of western New-York are enumerated in the order of suc-
cession; and, with some exceptions and omissions, the order is correct, and the subdivisions
will always hold good in the science. It is a remarkable fact, that at this early period, Mr.
Eaton should have recognized the sandstone of the Catskill mountains as the Old Red of
Europe; which, now that we have identified its characteristic fossils, is proved to be true.
Had he seized this grand idea, and confined himself to the elucidation of the strata below the
Catskills, he would have brought to light the most interesting series of rocks yet known in
any part of the globe. But in his examinations westward, the attempt to identify the Oneida
conglomerate with the Coal conglomerate, and the sandstone bordering Lake Ontario with
the New Red Sandstone, gave rise to that distortion of the geology which has prevailed regard-
ing the whole western portion of the State. The great source of error throughout seems to
have been the prevailing desire to identify, within the limits of New-York, all the rocks and
systems published in Europe from the Tertiary downwards. -
We cannot otherwise than regard it as a great misfortune that European systems were ever
made a standard for our rocks, which should have been studied and described as they are,
and as they always must remain the grandest development in the world, of the older fossili-
ferous formations. - , - -
Prof. Eaton had previously published his “Index to the Geology of the Northern States,”
in which he attempted to give a systematic classification of American rocks. He subse-
quently published two editions of a geological text-book, with many modifications regarding
arrangement, with which more recent observations do not concur. How far the rocks of the
State were developed, and their relative position shown by his labors, will be seen when
describing individual masses; and in all cases, the names by which he designated them will
be given among the synonymes, or adopted when applicable.
Prof. Eaton, in connexion with Dr. T. R. Beck, afterwards made an agricultural survey of
Albany county, in which all its mineral productions are described; and with Dr. L. C. Beck,
a similar survey of Rensselaer county. These labors led to the establishment of the Rens-
selaer School, under the patronage of Mr. Van Rensselaer ; the objects of the Institution being
PRELIMINARY CONSIDERATIONS. 7
to disseminate a knowledge of the natural sciences, with their application to agriculture and
the arts of life.
Besides the publications of Prof. Eaton, few have appeared in a separate form upon the
geology of the State. The other records of observation consist mostly of notices and com-
munications made to scientific journals and learned societies, and published in their transac-
tions. In these are preserved a very numerous collection of facts relating to the mineralogy
and geology of the State.”
Having been a pupil of Prof. Eaton in the Rensselaer Institute, and receiving there my
first instruction in Geology, it was natural to speak of him and his labors, as a tribute of
respect as well to himself as to Mr. Van Rensselaer, than whom no man more desired the
amelioration of human evils and the extension of knowledge.
To speak of all whose labors deserve the grateful remembrance of the student of nature,
would carry me beyond the proper limits of my subject; but two names which preéminently
claim a notice, are those of Dr. MITCHILL, the father of natural history in this State, and to
whom we owe the first collection of minerals brought to this country from Europe; and DE
WITT CLINTON, who, to every other distinction of greatness and excellence, added the most
enlarged views for the advancement of scientific knowledge.
We now come to the condition of the subject in New-York, previous to the commencement
of the survey in 1836. r
Very little detailed knowledge of the strata was possessed; a general idea of the order
among the principal rocks, with a more particular description of some places, being all that
was taught. The intimate relations and connexions of our series with the great Coal forma-
tion was not understood, and doubt and anxiety prevailed regarding the probability of finding
coal within the State.
The attempt at subdivisions among the strata had not been attended with entire success.
The slates and sandstones of the Hudson river group had been considered as the lowest rocks
of the Transition system; while the calciferous sandrock, and the limestones of the Champlain
and Mohawk valleys were supposed to lie above. This error arose from the influence of the
disturbing force, which has operated so extensively along the eastern border of the State;
dislocating, overturning and altering the strata to a great extent, and so disguising the lowest
stratified masses as to render it, at that time, extremely difficult or impossible to identify them
with the undisturbed and highly fossiliferous strata of the same group farther west. At that
time few observers had attempted to elucidate the order of superposition, and thus the subject
of their actual relations remained involved in doubt and obscurity.
The origin of the brine springs of the central and western part of the State was unexplained;
and the search after stronger water, or fossil salt, was conducted at hazard, regardless of the
conditions or situation of the materials giving rise to the springs. The position of the salife-
* A very complete list of these may be found in the Report on the Geological Survey, made by the Hon. J. A. DEX to the
Legislature in 1836.
8 GEOLOGY OF THE FOURTH DISTRICT.
rous rocks had not been clearly pointed out; and it was the general belief that these masses,
continuing westward from Salina, bordered Lake Ontario. In this manner two very distinct
formations were confounded with each other, and the mistake gave rise to much difficulty and
disappointment; for as the sandstone of Lake Ontario every where contained salt springs, it
was inferred, that by boring to a sufficient depth, water could be found of the quality of that
at Salina. Numerous attempts of this kind were made, and always resulted in failure, for
the reason that the former seems less abundant in saline matter than the latter, and also that
there is no situation along its range to act as a reservoir, like the great depression of the
Onondaga Valley. - - -
The difficulty of identifying strata at different and distant points, gave rise to many errors.
As an instance of this, the limestone of Black-Rock was always supposed to rest upon, and
constitute a part of the Niagara limestone, while the whole Salt group which intervenes had
been overlooked. This arose from the preconceived opinion that the Salt group was north of
the terrace at Lewiston, and consequently the two limestones in question could be separated
by no known rock.
In this state of things, it is not surprising that mining, and borings for salt water, should
have been made in all situations and in every rock. Having no guide in geological indications,
any situation presenting some remote analogies, or the existence of some peculiar substance,
was sufficient inducement to undertake extensive explorations; and had it not been that the
purse usually failed sooner than the zeal of the individuals, we might have had some fine
artificial exhibitions of our strata. *
As an example of the slight grounds upon which explorations are undertaken, it may be
mentioned, that almost every rock containing carbonaceous matter, or possessing bituminous
odor, has been bored or excavated for coal; and the presence of bitumen in any rock, is by
many considered an unerring indication of the existence of this mineral. Not less futile or ill
founded are the explorations induced by the presence of iron pyrites, or a few glimmering
scales of mica, which have given origin to mining operations on a small scale in innumerable
places. These illusions, however, are fast vanishing before the diffusion of more accurate
information, and a few years will see every one in possession of the requisite knowledge to
direct his inquiries aright.
In all attempts to reconcile the rocks of America with the geological arrangements of
Europe, the difficulties arose from certain remarkable differences between the formations
of the two countries; such as the existence of successive and extensive limestone deposits
in the eastern portion of the United States, with—as we have now learned—the absence of the
carboniferous limestone of Europe, the most important limestone there known as existing
below the coal. These limestones agreed with none at that time described, and as they pos-
sessed some general characters (containing corals and encrinites) in common with the carbo-
miferous limestone, they were referred to the same period.
A glance at the treatises on geology which have appeared in England during the last thirty
years, will give the history of progress in this part of the subject there, where so many
observers, with so great facilities, have been constantly at work. It must be recollected also
PRELIMINARY CONSIDERATIONS. 9
that these comparisons between the rocks of the two countries were made before the applica-
tion of organic remains to the identification of the age of rocks had become general, or even
known here at all. Mineral or lithological characters were at that time the principal means
of deciding this question, and it is well known how liable to error we become by depending
upon this character, for the rocks even of different parts of this State; how much more so,
then, when attempting to identify those of distant continents.
Again, while in Europe the older strata are much broken up and inclining at a high angle,
those of the same age in New-York are very little disturbed, and throughout more than a
thousand miles in extent westward, are nearly horizontal. Thus while seeking for these cha-
racters in our rocks, we neglected much more important evidence; and it has sometimes
happened that the same formation, in one place, from its horizontality referred to more recent
deposits, has in other places, where disturbed and upheaved, been referred to older ones.
This character of undisturbed horizontality over a great extent, in Europe and particularly
in England, always considered as indicating deposits of a newer age, maturally led to the same
conclusion here regarding our strata. At the present time, with all our guides, and which
have only been afforded within a few years, we can scarcely conceive the condition of the
subject during the earlier periods of observation in this country. From these facts, we learn
that no condition of rocks, in regard to greater or less degrees of disturbance, can be consi-
dered an indication of their age. We find in our country the oldest sedimentary rocks in their
natural or horizontal position, unaltered and undisturbed; while in Europe, deposits much
newer than the coal are so altered, that till recently they have been referred to the primary or
hypogene. - -
At the time our strata began to be studied, the doctrine of total destructions and renovations
was generally admitted; the termination of every geological period was supposed to be marked
by the annihilation of every living thing, and the commencement of the next one as distinctly
by a new and entirely different creation. Further observation has tended to the abandonment
of this doctrine; and so far as our knowledge now goes, there seems to have been a gradual
change from the first period of living things to the present time. Except in comparatively
limited districts, no sudden destructions or violent catastrophes have occurred; the loss of
species appears to be due to their gradually dying out, as the climate and condition of the
ocean became unfit for them; and the appearance of new ones seems, in like manner, to be
induced by changes causing a condition favorable to their existence.
Of the extinction of species, we have an example on our own coast at the present time, and
others might be enumerated. An extensive bed of the dead shells of the Pholas costata has
recently been found at New-Bedford, while it is unknown as a living shell on the shores of the
eastern or middle States." It is thus evident that this shell at one time existed in great num-
bers in a situation where, by some change unfavorable to its continuation, it has become
extinct.
* Dr. Gould's Report on the Invertebrata of Massachusetts, p. 27.
GEOL, 4TH DIST. 2
10 GEOLOGY OF THE FOURTH DISTRICT.
ſ
At one time fishes were supposed to date the commencement of their existence subsequent
to the Coal period; nevertheless, their remains have been traced downwards through the
Carboniferous system, the Old redsandstone, and into the middle of that vast fossiliferous
series of the older periods known as Transition or Silurian. In New-York, the remains of
fishes have been found in the Oriskany sandstone and succeeding limestones of the Helder-
berg series, holding a central place in the New-York system. From the facts now known, it
appears that trilobites were the first created animals possessing highly developed locomotive
powers; they being the “lords of the earth” till the appearance of higher organizations, as in
the fishes. Still, subsequent facts may reveal to us the astonishing truth that fishes were among
the earliest inhabitants of the globe, and thus that vertebrated forms held place among the
first creations.
Scarcely less erroneous was the opinion promulgated that the fossil remains of the older strata
consisted of a few singular crustaceans with brachiopodous shells, or such as possessed an
opening under the beak for the protrusion of a peduncle by which to attach themselves, as in
Delthyris and Orthis; together with some singular forms of chambered shells, as Orthocerae,
and others; and that the whole assemblage was so unlike the Fauna of the present ocean,
that there was nothing existing with which to compare them. On the contrary, though the
greater number as regards species and individuals are of types quite distinct from the most
of those inhabiting the present ocean, yet we now know that several of the fossil genera of
the older rocks are still living in our seas, having existed through every geological era. A
species of the genus Lingula appears in the oldest known fossiliferous rock; and this shell,
with Orbicula, were among the earliest inhabitants of these ancient waters. In rocks of the
same period, we find shells closely allied to, if not identical with, Trochus, Turbo, Buccinum,
Nucula, Avicula, and numerous other genera; while among the living crustaceans of the
southern hemisphere, are forms closely allied to the trilobites of this period. In fact it would
appear that in these earlier deposits are an assemblage of fossils, as much like the Fauna of
the present seas as in some of the subsequent geological periods.
The doctrine of violent catastrophes, and of sudden changes in the inhabitants of the ocean,
was based upon the examination of limited districts, where the entire series of deposits had
never existed, or had been subsequently obliterated. And gradual and tranquil as the changes
now seem to us, they may appear infinitely more so when a perfect sequence among the
strata of the whole globe shall become known—when a complete succession shall be esta-
blished from the oldest to the newest rock. From what we now know, compared with the
knowledge existing a few years since, we can readily infer that some distant places, or even
nearer localities, may furnish links now wanting in the chain. -
In learning to regard nature as always the same, and her laws unchanging, we have made
a grand step towards the explication of phenomena before unexplained, except through a sus-
pension of the natural laws, or a miraculous interposition of creative power. Nature is always
perfect and unvarying, but man's knowledge is progressive; consequently in every advance
he arrives nearer to the truth, and yet as far from knowing all nature and her laws as he is
from Infinity.
PRELIMINARY CONSIDERATIONS. II
The knowledge of mankind, therefore, at one age seems but as folly or ignorance in a suc-
ceeding one; and it is the same regarding our own knowledge at different periods. Still
there are certain principles which never fail, and which man through his whole life, and
mankind throughout all ages, have acknowledged as fixed and unalterable. It is not the facts
of observation that change, but the inferences which we draw from them, as our knowledge
becomes more extended, and facts before unknown are added to the stock.
Exact knowledge, therefore, consists in those things which can be seen or demonstrated;
while in all knowledge of inference, there is progression. Opinions which are often the result
of imperfect knowledge are liable to change, and the human mind is never advanced by adopt-
ing the opinions of others; for by that means, man is never made a thinking being, but rests
upon authority. 2. '
Viewing nature and the mind of man in this light, we are not to look at the imperfections
in the works of those who preceded us, but to be satisfied to add a few more facts to the great
store of exact knowledge. We are to consider always that theories and systems are merely
an exposition of the present amount of knowledge on the subject; and that science is the
term used by philosophers to designate the conclusions drawn from a systematic arrangement
of facts, verified by other facts, relating to any portion of nature's works; not in the least
signifying that man's knowledge is perfect in any department of nature, or that science is less
susceptible of improvement by the addition of new discoveries.
In all sciences, the acquisition of new truths exhibits in new light the beautiful operation
of the laws of nature; and in none more than in geology does it show them operating in a
uniform and unvarying manner through successive periods, as proved by the organic contents
of the strata of every geological era. In no science have facts accumulated more rapidly;
but it is within a comparatively recent period that these have been rightly interpreted, or have
led to the simple and satisfying, and at the same time stupenduous conclusion, that nature
has been operating through incalculable periods of time, with the same harmony and unity
of design as we behold in her present creations. .
The history of geology in our own country, even for a few years past, and within the
memory of almost every one, shows how rapidly the subject has advanced, till from a word
scarce comprehended, the application of its principles are of daily adoption among us, and
the results of its investigations known to all.
I? GEOLOGY OF THE FOURTH DISTRICT,
CHAPTER II.
General Features of the Strata, Topography, etc.
IN describing the rocks of the Fourth Geological District, according to their physical or
lithological characters, and the effects of these in modifying the contour of the surface, we
shall find the whole area occupied by several successive parallel groups or associations of
strata, each possessing characters which distinguish them from others above and below. The
general line of their bearing or strike is nearly east and west, with some slight variations
owing to denudations, but never to uplifting or derangement. This will be clearly seen on
reference to the colored geological map. Throughout the whole distance, there are no dis-
turbances of much importance; and the greatest effects produced in any case, are slight dis-
locations extending for a few yards; or sometimes gentle undulations of the strata, which may
affect them for several miles. To this character of the country we owe its great simplicity
of structure, the order of succession being scarcely any where obscured except by superficial
detritus. This in many places, and for considerable extent, covers the nearly horizontal
strata, and in some instances renders the local succession obscure. Still the numerous river
channels and ravines, the deep excavations of the north and south lakes, all aid in developing
in the most satisfactory manner the whole series from the highest to the lowest rock. And
although we have not to describe the great changes and important modifications wrought
upon the strata by plutonic agency, yet we have exhibited in the most perfect manner the
natural arrangement of the deposits, the situation and condition in which they were left by
the agents of their production; and we can recognize, unchanged by subsequent influences,
the nature of deposits at remote points from each other. We trace a rock through all its
grades of coarser materials to finer and finer, until at last we find it composed of comminuted
matter which slowly sank to the bottom in the deeper parts of the ocean.
The analogy to recent formations is thus more fully seen; for we have precisely the same .
materials, differing only in degree of induration. We have the unaltered monuments of a
wide spread ocean teeming with life, and we find recorded its changes through vast periods
of time. We now learn what were the conditions of its bed at these successive periods, and
also what different characters it presented at distant points. The varying forms of its inha-
bitants are as well marked and as perfectly preserved, as the recent species amid the mud
and sand and pebbly bottoms of our present seas. The geographical limits of certain genera
FEATURES OF THE STRATA. 13
and species are as well defined in that primeval ocean, as in the present; and as now, upon
the same bottom, we find in some places great accumulations of organic forms, while in others
they are rare or wanting. Like our present ocean also, we know that this ancient one was
agitated by winds and moved by tides; the drifted shells and comminuted corals tell us
plainly of waves and currents, while in other places the fine sediment and equally distributed
organic remains speak either of a quiet sea or deep water, where they were placed beyond
the tumult that might have raged nearer the surface.
It is scarcely possible that the organisms of successive epochs could have been preserved
in greater integrity than throughout the series, not only in our limited district, but over the
whole State, and far westward to the Mississippi river; upon whose banks, and those of its
tributaries, we find such an abundance of forms, as perfect almost as the living Naiades of
these streams, which derive the material of their habitations from the destruction of these
ancient deposits.
In its great topographical features, this district presents the following view : Bordering Lake
Ontario on the north, is a low plateau, gradually rising to the south for a distance varying
from four to eight or nine miles, where we abruptly ascend a terrace, which at its western
extremity attains a height of two hundred feet, but which slopes gently down almost to the
general level farther east. From the top of this terrace, we pass over a broad plateau of nearly
level country, slightly depressed towards the centre, but rising gently again to the south till
we come to the base of a second terrace, having a general height of sixty feet or more above
the country on the north. These two terraces correspond with the outcrop of the two great
limestone formations, the southern one extending throughout the State, forming a prominent
feature from the Hudson to the Niagara river. Beyond the terrace last mentioned, the coun-
try is level and generally even for several miles, when we commence a gradual ascent to
higher ground. Here, however, there is no definite line bounding the northern extension, as in
the case of the two terraces; but the outline is irregular, projecting in one part and receding
in another. We find ourselves upon the margin of a country composed of hills and valleys,
having no general direction other than that given by the water courses. Although the coun-
try to the south of this is hilly, and in some parts rising to an elevation of twenty-five hundred
feet above the ocean, yet it must be remembered that there are no ranges of mountains; the
whole surface is equally and alike covered with elevated plateaux, without the possibility of
limiting any of them as to course or direction. The deepest valleys being north and south,
give this apparent bearing in some places to the neighboring hills.
Having no indications of disturbances or upliftings, we are therefore to look to another
cause for the production of these hills. We must fancy this whole southern border of the
State as having once been a high and broad plateau, with the underlying rocks extending
much farther to the north, uniform in outline and even in surface as the limestone terraces
just described; and that from denudation, the breaking up of the strata in some places, to-
gether with the action of waves and currents, has resulted this irregular and uneven surface.
As proof of this, if we examine the strata on the two sides of a ravine, we shall find that if
14 GEOLOGY OF THE FOURTH DISTRICT.
continued they would meet in the same plane; and pursuing the same course in regard to
near or distant hills, or across broad valleys, we find invariably the same rule to hold good.
These features are produced only by the removal of the mass which once filled the space,
precisely in the same manner as those made by the excavation of roads through ridges of sand
and gravel; the power in this case being that of nature over a great extent of surface, and
in the other that of man over a very small one. All these hills are termed in geology outliers,
or continuations of the same strata, where some intervening portions have been removed.
The larger streams flow in the deepest valleys, while the intermediate portion of country
is less excavated, and presents eminences less abrupt. Much of the higher ground, indeed,
exhibits a surface with gentle eminences and broad valleys, bounded by low hills equally
extensive. This character is more extreme toward the southern limit of the State; and on
going northward, gradually diminishes, the undulations becoming more gentle, until finally we
come upon an almost unbroken level. -
Further examination will show that each change in the topographical features is due to a
change in the underlying rocks, and that the same rock does not give rise to any two of the
main features described. The place and limit of certain formations are thus indicated upon
the surface, and afford a general guide to the observer; though he will find less important
changes in the strata not affecting the external form or character of the country. The thick-
ness or extent of a rock, also, has great effect in modifying the external exhibition; while
thin masses of different kinds may exist interstratified with thicker ones, and the whole sur-
face carry the character of the predominating rock.
On investigating the lithological character of the strata of this district, we shall find that
their varied composition and texture has given rise to the great features of its surface; and
that hence is due not only those pleasing and beneficial inequalities, but also the origin of the
streams and water falls which beautify and enliven the scenery, while they offer encourage-
ment to enterprise and industry, which in a country less diversified would never be called
into action. We find the first plateau, or that bordering Lake Ontario, underlaid by a soft
friable or shaly sandstone, having nowhere, except in its higher members, sufficient firmness
to resist the universal denuding action which has formerly prevailed far beyond the limits of
this district. Accordingly it is evenly worn down, and presents few varied features, except in
the river channels. Through Wayne and a part of Monroe counties, a portion of this gentle
slope toward the lake is underlaid by some thin beds of limestone with alternating and suc-
ceeding shales, giving no different aspect to the surface. Through this part of the country,
also, the terrace bounding the plateau is scarcely defined, forming merely a slight elevation
above the country on the north. Westward from Rochester, it becomes a prominent feature;
and the shales just alluded to form its abrupt northern slope, increasing in height as we go
westward. The platform of this terrace is a thick mass of limestone, which has resisted the
influences that levelled the shale and friable sandstone on the north; and it now presents its
line of strike in bold relief, extending from Rochester to the Niagara river at Lewiston, and
far beyond into Canada.
TOPOGRAPHY, 15
Again, this limestone is succeeded by soft marls and shales which have been levelled by
the denuding agents, and present the second broad plateau. This is again limited on the
south by a mass of limestone, sufficient to resist the power that wore down the others. Suc-
ceeding this limestone, are in turn soft shales, forming for some miles a level country, and
the next ascent is produced by the interstratification of harder layers of sandstone. These strata
of sandstone being thin, prevented the entire levelling of the shale, but did not produce the
well defined outline presented by the limestone; consequently we have the gently swelling
hills, gradually receding, and the contour softened in the undulating curves which mark the
windings of the streams. -
Such are the principal features of a portion of country, the rocks of which we are about to
describe. -
Connected with, and dependent upon this character of the surface, are other circumstances
to be noticed. The form of the country, determining the direction of the present water
courses, is a matter of great importance. The highest portion of this district is occupied by
the counties of Chemung, Steuben, Allegany, Cattaraugus and Chautauque, the mean eleva-
tion of which is about two thousand feet above tide water. The northern portion of this range
forms the dividing ridge of the principal streams flowing in opposite directions, which mingle
their waters with the ocean at distant points. Those on the north find their way into the
Atlantic by Lake Ontario and the St. Lawrence river; while on the south, some flow into
the ocean by the Susquehannah, and others passing into the Allegany, find their way to the
Gulf of Mexico by the Ohio and Mississippi. The Genesee is an exception to the general
rule — a river which takes its rise beyond the borders of the State, and flows northerly through
all these counties, and discharges its waters into Lake Ontario. A river of this magnitude
passing through a great succession of strata, and descending in all its course nearly two
thousand feet, has produced some grand exhibitions of the rocky strata.
Valleys similar to that of the Genesee, cross the district in a north and south direction;
the principal of these are occupied in part by lakes, as Cayuga, Seneca and Canandaigua ;
the valleys in all cases continuing to the north and south of the extremities of these lakes, but
the direction of the water courses being opposite from the highest part of the valley which is
south of the lakes. These ancient water courses, with the great lakes and the river dis-
charging all the western waters through its narrow gorge, while they modify the topography,
form some of the most striking features of the district, and are subjects of the highest interest
both to the man of science and the utilitarian. -
To the same cause, to which we owe these prominent features and the hills of the southern
counties, is also due the deep fertile soil prevailing throughout the greater part of the district.
The materials excavated from these valleys in the form of fragments and masses have been
transported and reduced to the condition of sand, clay and pebbles, which is distributed over
the surface. By the same operation, also, the materials of the northern calcareous strata are
mingled with the comminuted rocks of the south, and form the soil of unsurpassed fertility
16 GEOLOGY OF THE FOURTH DISTRICT.
which supports the heavy forests, and produces the abundant harvests which render western
New-York the garden of the State. . - - .
The high hills and deep valleys indicate the absence of an immense quantity of matter,
which, during the same period, was transported in the direction of the great outlets into the
present ocean, there to lay the foundation of future continents in strata like those occupying
our district, filled with the organic remains of successive ages, and exhibiting throughout
their extent all the varying characters that we now find in the rocky strata of our continent.
TABULAR VIEW, 17
CHAPTER III.
Tabular view of the rocks and groups described in the Geological Reports of New-
York; their extent, and agreement with those of Europe.
Geographical or local names having been employed in the annual reports for designating
the different sedimentary deposits, the extension of this idea led to the adoption of the term
NEw-York SystEM, including all those masses so well developed in the State, defined below
by a well known line of demarcation, and terminating above with an equally well ascertained
limit, viz. The Old Red Sandstone. In all this series, there are no limits by which subdivi-
sions could be indicated, of sufficient importance to entitle them to the name of systems.
The term thus becomes purely geographical, leading to no theoretical considerations what-
ever, being no favorite of individuals, but a consequence of the superior development of the
strata included in that System, as brought forth by the geological survey of the State. The
names which designate formations of the same age in other countries, are found inapplicable
to our rocks; and by adopting the term New-York System, all ambiguity respecting its signi-
fication is avoided.
Below is a tabular view of the systems and groups adopted by general consent for the rocks
of the State, and followed in all the Reports with no important variations. The names have,
with few exceptions, been derived from well known places, where the rock is best developed,
indicating in all cases an important point for the investigation of observers. In most in-
stances where names had been previously applied, and concerning which there was no
ambiguity, they have been retained.
I. PRIMARY OR HYPOGENE SYSTEM.
Including granite, gneiss, hornblende rocks, etc.
II. TACONIC SYSTEM.
, Represented by the Taconic range of mountains in the castern part of New-York.
GEOL. 4TH DIST. 3
18 GEOLOGY OF THE FOURTH DISTRICT.
III, NEW YORK SYSTEM.
This includes all the products between the Taconic and the Old Red Systems, commencing with the
lowest known sedimentary rock, and terminating at the base of the latter.
Under the New-York System are included the following rocks and groups, in their order of succes-
sion : -
\
Geographical subdivisions. Systematic subdivisions, founded upon the fossil and lithological
. | - characters.
yº- T 1. Potsdam sandstone.
2. Calciferous sandrock. -
3. Black-river limestone group, embracing the Chazy
and Birdseye. -
CHAMPLAIN DIVISION. × 4, Trenton limestone,
5. Utica slate.
6. Hudson-river group.
7. Grey sandstone.
8
8. Oneida or Shawangunk conglomerate.
? { 9. Medina sandstone,
ONTARIO Division, -- 4 10. Clinton group.
11. Niagara group, including shale and limestone.
ſ 12. Onondaga-salt group.
13. Water-lime group.
14. #º º:
- 15. Delthyris shaly limestone.
Nº. K < 16. j i.
g HELDERBERG SERIES. 4 17. Upper Pentamerus limestone.
18. Oriskany sandstone.
19. Cauda-galli grit.
| 20. Schoharie grit.
21. Onondaga limestone.
22. Corniferous limestone.
ſ 23. Marcellus slate,
- Moscow shales.
24. Hamilton group. & Encrinal limestone.
llv I }; shales.
- 25. Tully limestone.
ERIE Division, ----- { . tº. slate.
2 . Portage sandstone.
27. Portage or Nunda group, X Gardeau flagstones.
..” Cashaqua shale.
L28. Chemung group.
TABULAR VIEW, . - 19
IV. OLD RED SYSTEM, OR OLD RED SANDSTONE.
This division includes those rocks forming the greater part of the Catskill mountains; and extending
westward, they disappear near the Genesee river.” The remains which mark this division, so far as
yet known, are principally those of fossil fishes; two species only of shells having been found. Fucoids
and fragments of land vegetables are abundant.
W. CARBONIFEROUS SYSTEM.
Of this System, but a single member, the lowest of the series, occurs in the State; unless it may be in
the counties o Delaware and Sullivan.f This member, the conglomerate, forms numerous outliers in
the Fourth district, always, however, isolated, and of small extent; no rock in the series above being
visible, - w
WI. NEW RED SANDSTONE.
This formation extends within the State, occupying a portion of Rockland county, and being a con-
tinuation of the same rock more extensively developed in New-Jersey.
VII. TERTIARY.
Including the blue and yellowish clays, and their fossils, of the Champlain and St. Lawrence valleys.
VII. QUATERNARY SYSTEM.
This system includes all the superficial deposits of the State, except the Tertiary, and may be arranged
under the following heads: -
Including gravel, sand, clay, etc.; being all that class
1. TRANSPORTED MATERIALs,. . . . . . . . . . . . . . . . . . . of deposits which are usually known by the names dilu-
vial, alluvial, drift, etc. - - * .
Peat, muck, lake marl, tufa, bog ores, and soil formed
2. LoCAL DEPoSITs, . . . . . . . . . . . . . . . . . . . . . . . . . . . from the decomposition of rocks in place; fossil bones of
mastodon, etc.
* Since the numerous investigations in Europe have proved the Old Red Sandstone a system distinct from the lower rocks, it
seems premature, in our present state of knowledge of that rock in this country, to merge it in the New-York System; particu-
larly since those points which have served to identify the rock with the Old Red of Europe, certainly contain a very distinct assem-
blage of organic remains from the groups below. The rocks occupying the Catskill mountains, though evidently of the same age
as the sandstone yielding remains of fishes farther west, have as yet produced no organisms of this kind; and further examina-
tions must settle the question regarding the propriety of their union with the New-York System.
# It must be remembered that we have no limestone within the limits of the State, equivalent to the carboniferous limestone of
Europe; and therefore the lowest member of the System spoken of, is the lowest member as the series is known to us in New-
York. Farther west, however, there is a limestone, holding the place of the carboniferous of Europe, which passes beneath
the conglomerate; both of these are well exposed on the Ohio river, and in many places in Indiana and Kentucky. If this lime- º
stone be regarded as a part of the Carboniferous System, the conglomerate, which in western New-York and some parts of Ohio
rests upon the Chemurg group, must be considered the second member in the ascending order.
20 GEOLOGY OF THE FOURTH DISTRICT.
The New-York System includes rocks, which, in Great Britain, have received three dis-
tinctive appellations: 1, The Cambrian System of Prof. Sedgwick; which, judging from
specimens, includes rocks lower than the Utica slate, and apparently similar to the disturbed
strata along the Hudson river, though probably not reaching so low as the Potsdam sandstone.
2, The Silurian System of Mr. Murchison; which embraces the rocks and groups from the
Utica slate to the Hamilton group, and so ably and beautifully illustrated by that author.
3, The Devonian System of Prof. Phillips; which appears, from the numerous illustrations
of its fossils, to correspond to the Chemung and Portage groups, and also to include a portion
of the Hamilton."
The Devonian System, as usually understood in this country, is supposed to include the
Old Red Sandstone of Europe; but in central New-York, there is a well defined line of
demarkation between the Chemung group and the Old Red, which contains remains of the
Holoptychus, &c. Many of the fossils figured by Mr. Phillips are identical, and others very
similar to those of our Chemung and Hamilton groups, while they differ widely from those of
the Catskill, or Old Red Sandstone. * ^
From the absence of all extensive disturbances of the strata, we are enabled to trace an
uninterrupted series from the Potsdam sandstone to the Old Red. No where is there known
to exist so complete a series of the older fossiliferous rocks, as those embraced within the
limits of the State; and terminating at a point of great and important change in the condition
of the surface, and included between this and the rocks of metamorphic origin, we have here
offered one of the most decided and best characterized systems known in the whole world.
The New-York System thus becomes equivalent to what was embraced in the Transition
by Werner, which term in modern times has been found too objectionable to retain. It like-
wise includes the three systems of English authors just mentioned, leaving the Old Red
Sandstone and Coal to a subsequent period. And this for the reason, that in New-York,
where the means of investigation are best afforded, and where the whole series is undisturbed,
there is manifested the most complete and continuous succession; showing but one geological
era for the deposition of the whole. In that era, the earth first witnessed the dawn of animal
life, and ages of its greatest fecundity in marine organisms; and the approach of the period
when it became fitted to support a vegetation so luxuriant and universal, of which no modern
era affords a parallel. - &
Hitherto great confusion had prevailed regarding the rocks here enumerated as occurring
between the Carboniferous and Primary series; and it was not until the publication of the
result of Mr. Murchison's labors, that we had any definite knowledge of the sequence, in other
places, of these extensive groups, which over thousands of miles in area are the most impor-
* Since writing the above, I have received Mr. Murchison's Address before the Geological Society of London, (1842,) and he
there distinctly states that the Devonian System constitutes a portion of the Silurian, and is inseparable from it. This view accords
perfectly with the facts here stated. In the same Address, the Cambrian System, as distinct from the Silurian, is no longer
sustained; and the reasons are given which led to its adoption, as well as those for its abandonment. The views which have
been long entertained here in New-York are thus unexpectedly corroborated, and the results will doubtless prove auspicious to
the science.
TABULAR VIEW. 21
tant rocks of our country. Heretofore they had all been termed Transition or Greywacke,
and no successful attempt at subdivision had been made by any European geologists; while
in this country, as before mentioned, all efforts had been to identify them with the published
systems of Europe. Mr. Murchison's work therefore shed a flood of light upon what had
previously been a region of darkness, and gave confidence to those whose examinations were
directed towards the subject of elucidating these deposits. .
In the Annual Report of 1840, I expressed the following opinion of the value of that work
to the American student in lower geology: • -
“Since the publication of Mr. Murchison's work, we have been enabled to establish with
“great certainty, the analogy of our rocks with those of the Silurian System, as developed
“in England and Wales. In this country, however, the greater undisturbed range, and ap-
“ parently better development of particular members, with more numerous species of organic
“remains, enables us to limit our subdivisions within narrower bounds, and thus offer greater
“facility for the study of particular groups.”—“It forms an era, and an important one in
“ the development of the older fossiliferous rocks, which have been so long enveloped in
“obscurity. It offers inducements to the study of the same, which have never before been
“presented; since, particularly in this part of our country, the rocks of the Silurian System
“are better developed than any others; while the means of studying them with guides have
“been entirely wanting. Thus the student, after weary months of labor, abandons the sub-
“ject in despair, being unable to identify the rocks or fossils with any system heretofore
“published; and having made too little progress to systematize the whole, distrusts what he
“does know, because it seems inapplicable to what he supposes the same rocks or their
“equivalents in another county.” Mr. Murchison has done for the older deposits what Mr.
Lyell has done for the more recent; and we have now in each system standard groups of
reference, which, so far as examinations have progressed, hold true over extensive districts
of country. -
Mr. Murchison, in company with M. de Verneuil, has since been investigating the same
formations in Russia; and he mentions, in a letter, the occurrence of rocks in Siberia,
charged with Pentamerus Knightii, a fossil abundant in a particular position in England.
Formations of the same age have long been known in Sweden and Norway, Canada and va-
rious parts of North America, extending far westward; and during the past year, I have traced
the groups as developed in New-York, throughout the country intervening this State and the
Mississippi river, and thence into the territory of Iowa. The occurrence of fossils typical
of the lower part of this great series, shows its extension over an extremely wide area.
Fossils from Lake Huron, Lake Winipeg, and several points of the far northwest, all indi-
cate the existence of rocks equivalent to the Lower Silurian of England, or the Champlain
division of New-York. Mr. Stokes, in a paper “On some species of Orthocerata.” publish-
ed in the Geological Transactions, speaking of the localities, and the circumstances under
which they were collected, remarks: “It will be observed that these American localities are
“widely separated from each other, and are not parts of a continuous deposit; but the agree-
“ment in character of the limestone rock, and of the fossils, shows that they are of the
22 GEOLOGY OF THE FOURTH DISTRICT.
“same geological age.” From examinations made in the eastern part of Maine, New-
Brunswick, Nova-Scotia and Canada, by Messrs. Jackson and Alger, Capt. Bayfield, Dr.
Emmons and others; and from the examinations of Bigsby on Lake Huron, of Houghton in
the northern and southern peninsulas of Michigan, and of Owen upon the Mississippi river;
together with facts collected from others, and having also passed over much of this ground
myself, as well as of some intermediate points, it appears that there is an almost continuous
deposit of the lower rocks of this great system entirely across the continent, from the Atlantic
to the Pacific oceans. Thus ever an extent of more than half the circumference of the globe,
the existence of these older fossiliferous rocks has been proved; and from being a neglected
and unarranged mass, they seem likely to assume the first rank in importance among geolo-
gists of the present day. - -
Notwithstanding the remarkably persistent character of the lower formations of this great
System, I am able to state from personal observation that the higher groups thin out rapidly
in a western direction from New-York. The rocks above the Helderberg series, known in
New-York as Marcellus slates, Hamilton, Portage and Chemung groups, and some minor
subdivisions, altogether forming a mass of more than three thousand feet in thickness, have
diminished to less than as many hundreds before reaching the Mississippi river. At the same
time, the rocks forming the principal part of the Catskills, and being in part or the whole
equivalent to the Old Red Sandstone of Europe, together with several members of the Helder-
berg series, have disappeared in a western direction within the limits of the State of New-
York. The wide spread and generally uniform character of the one, proves a similarity of
circumstances throughout; while the great difference in thickness, and the absence of fossils
in parts of the other, proves a great difference in the conditions under which they were depo-
sited at different points. We shall probably find that the remark heretofore made, that “the
older deposits are the more universal,” will hold true, not only as regards the great systems or
classes, but also the minor subdivisions. It exhibits in the commencement of the organic
period, a uniformity in depth and temperature of the ocean, or other circumstances favorable
to the development of the same forms over vast areas, which in subsequent periods have
constantly diminished. -
While the investigations have been going on which have resulted in the development of the
rocks of New-York, as exhibited in the tabular arrangement, we have had fellow laborers in
other parts of this great field. Other States have pursued the same course; and from the
numerous and efficient observers, we have accumulated a great amount of knowledge regarding
the geological structure of the whole Union.
In Maine, the Primary and lower fossiliferous rocks have been investigated by Dr. Jackson,
and also the Primary and Coal measures of Rhode Island, and the Primary of New Hamp-
shire.
In Massachusetts, after the publication of the report of the first survey, a resurvey was
ordered; and Prof. Hitchcock has just completed two quarto volumes, giving the results of
his researches in the Primary, some isolated tracts of the Carboniferous, New Red Sandstone
of the Connecticut valley, and Tertiary upon the coast. -
TABULAR VIEW. 23
In Connecticut, Dr. Percival with Prof. C. U. Shepard have investigated the geology and
mineralogy of the State, which includes the Primary, New Red Sandstone and Trap.
In New-Jersey and Pennsylvania, Prof. H. D. Rogers, and in Virginia, Prof. W. B. Ro-
gers, have been occupied in exploring the formations from the Primary, through all the older
fossiliferous rocks, the Carboniferous period, New Red, Oolite, Greensand and Tertiary.
In Maryland, a geological and topographical survey of the State has been in progress for
several years, by Prof. Ducatel and J. H. Alexander, Esq., and the work is now nearly com-
pleted: a local survey of the coal region of Alleghany county has been made during the past
summer, by Prof. Aikin. f -
Prof. W. C. Booth has made a geological survey of Delaware, giving a complete account
of all its formations and mineral productions. -
In the Ohio survey, under the direction of Mr. Mather, the reports of Dr. Locke, Messrs.
Whittlesey, Briggs and Foster, have elucidated in a great measure the geology of the State.
Dr. Hildreth had previously done much towards illustrating this subject, and his valuable
papers in the American Journal of Science are fully appreciated by those who have any know-
ledge of these formations in the west. - a
In Michigan, Dr. Houghton has been actively and zealously engaged in prosecuting to its
completion, a very thorough survey.
In Indiana, Dr. Owen, under the direction of the authorities, and partly upon private en-
terprise, has developed the great geological features of that State; and, with Dr. Locke, has
more recently been engaged in the lead region of Illinois, Wisconsin and Iowa.
In Tennessee, Dr. Troost has been for several years engaged in a geological survey of the
State, which has developed an interesting series from the Primary upwards.
Mr. Nicollet has recently been investigating the formations west of the Mississippi, and his
discoveries in that region have proved highly satisfactory and important.
In Georgia, Dr. Cotting has completed a survey of the State, and published a report upon
its mineral productions. -
North and South Carolina had been previously investigated by Professor Olmsted and Mr.
Wanuxem.
It will thus be seen that much the greater part of the territory east of the Mississippi river
has been partially or entirely explored under the direction of the respective State governments.
The remainder, will doubtless soon be investigated, either under the same auspices, or by
private enterprise. Much yet remains to be done in the way of harmonizing views, and
bringing the nomenclature to some general standard. For as these surveys have mostly been
pursued quite independently of each other, it has led to the adoption of terms, which, however
applicable, cannot all be well retained without overburdening the science with synonyms.
The comparative development of the rocks and groups in different parts of the Union, will
probably be the test of nomenclature; since local or geographical names have been generally
adopted, and at the present time meet with most favor. - -
The results of all these investigations have proved the existence of the rocks of the New-
24 - GEOLOGY OF THE FOURTH DISTRICT.
York System over the greater portion of the country between the grand Primary chain on
the east and the Mississippi river. And it further appears that throughout all this extensive
area, these formations are overlaid by no rocks more modern than the Coal formation, except
in a few limited districts where the newer Secondary rocks or those of the Cretaceous group
succeed the latter. Such wide development and generally undisturbed condition will cer-
tainly afford the means of bringing to light many important facts regarding the formations,
which could never have been known from the examination of limited districts, however perfect
the sequence. As before remarked, the territory of New-York, from possessing the most
complete series, and abundance of fossils, together with the undisturbed position of the strata,
offers the most interesting field of investigation and reference, and will be found the best point
of departure for the geologist who is making more extended researches. -
The geographical divisions in this table, though convenient for reference, nevertheless do
not indicate any great natural divisions of the system as founded upon fossil characters. Such
a mode of subdivision will follow only a perfect knowledge of the fossils, both in this State
and elsewhere. From the commencement of the fossiliferous rocks, to the termination of the
Hudson-river group, there seems to have been a uniformity of condition and a continuation
of species which cease with this period, and cannot be found in any subsequent one. The
two lower masses, it is true, so far as examined, contain few fossils, and those of species
not known to extend upwards; but these rocks must be considered as having been produced
at the dawn of that era, and are emphatically the “protozoic rocks;” while, after living
forms had become abundant, many of the same continued throughout the whole period unde-
stroyed. -
Mr. Conrad is disposed to include in this period the Medina sandstone and Clinton group.
The former possesses many analogies, though none of the fossils of the lower rocks; while,
on the other hand, none of the fossils of the Medina sandstone are continued into the rocks
above, and the apparent continuation of the Grey sandstone into the base of the Medina would
argue in favor of placing the latter in the lower division. But in regard to the Clinton group,
its great contrast with the Medina sandstone, both in lithological and fossil characters, seems
an insurmountable obstacle in the way of uniting this with the lower division; particularly
as in many points that group, or its fossils, pass into the next above, while we have not a
solitary example of the passage of any fossil from the lower group into this. The termina-
tion of the Medina sandstone, therefore, as far as regards the State of New-York, must be
considered the termination of the lower division of the system.
Throughout a part of New-York, and more particularly in Pennsylvania and Virginia, as
we learn from Professors H. D. and W. B. Rogers, the Oriskany sandstone forms a marked
line of separation, and might perhaps well be considered the limit of the Second great divi-
sion. Nevertheless, the absence of this rock in western New-York, in Canada, and, so far
as I know, in Michigan, Ohio and Indiana, would still render it an obscure point of reference.
The “Cliff limestone” of Ohio, which is there known as a single formation or group, includes
rocks both above and below the Oriskany sandstone. This shows such a close analogy in
the strata, that together with the absence of the rock on which the division is to be founded,
TABULAR VIEW. 25
it seems more natural to bring all the limestones into the second great division. Throughout
the region noticed, the upper limestone of the Helderberg series, the Corniferous, would
form a much more obvious termination of the second division. This is every where recogni-
zable, and thence upward to the Carboniferous, the rocks are marked by an entirely different
assemblage of organic remains. In the Helderberg series, where well developed, the line of
division, if dependent upon fossils, can be made at one point as well as another; few of the
forms rising above the group of which they are typical.
This arrangement would leave all the shales and thin-bedded sandstones of the succeeding
groups to form the Third and last division of the System; being a natural lithological assem-
blage, and also palaeontological, if specific characters are considered.
Another advantage to be derived from this arrangement is, that the great dissimilarity of
the products of the different divisions would lead to no confusion, as might result if some of
the limestones are left to be grouped with the shales; the latter being very meagerly fossilife-
rous in the west, while the limestones are highly so.
The middle division would embrace groups exhibiting a considerable diversity of fossil
characters, yet all possessing forms bearing a generic identity. The different groups, as
exhibited in the tabular view, with their fossils, to be enumerated in another place, will show
the character of this division of the system. These three divisions would be easily recognized
from the great change in lithological character, as well as extinction of fossil species, at the
termination of each one.
GEOL. 4TH DIST. 4
26 GEOLOGY OF THE FOURTH DISTRICT,
CHAPTER IV.
Enumeration of the rocks and groups below those of the Fourth Geological District,
ân the order of succession.
The rocks occupying the Fourth District commence at about the termination of the lower
great division of the System ; a point above which, few or none of the previously existing
organic forms are continued. The rocks and fossils of the lower division are described in the
reports of the First and Third districts; and they are merely enumerated here in the order of
succession, for the purpose of showing their connexion with those of the Fourth district, which
terminate above with the conglomerate of the carboniferous period. The report will thereby
be rendered more complete and satisfactory in itself, affording means of reference to the rela-
tive situation of the lower rocks, and of comparing the genera and species of their fossils
with those above.
The want of some previously acknowledged base line, from which to make the starting
point, has been felt during the whole of the survey; and to supply in some degree this defi-
ciency, I have examined the lower rocks upon the north side of Lake Ontario. These show
a continuation of the lower groups as developed in the eastern part of the State, with the
exception of that portion occupied by the basin of the lake. This, between the Fourth dis-
trict and the Canada shore, has been excavated partially from four of these groups, viz. the
Utica slate, Hudson-river group, and Grey sandstone, as well also as a large portion from the
Medina sandstone, which forms the southern border of the lake from Oswego to its western
extremity, and its northern margin for many miles near the western termination.
From these facts, it will appear that a section extending across the Fourth district, and
embracing the rocks upon the north side of the lake as far as the Primary range, will give a
connected view of all the rock formations presented farther east.
The following woodcut will illustrate these remarks. It shows the relative position of all
the rocks of the Fourth district, as well as their relations to the lower ones, in a section ex-
tending from the Primary of Canada, across the lake, and thence across the State of New-
York from the mouth of Genesee river to the Pennsylvania line.
LOWER ROCKS AND GROUPS, 27
A. Primary. - - L. l. Niagara group.
B. Potsdam sandstone, M. Onondaga-salt group.
C. Calciferous sandrock. N. Helderberg series.
D. Black-river limestone. r O. Hamilton group, including Marcellus slate and
E. Trentom limestone. Moscow shale.
F. Utica slate. e. Tully limestone. -
G. Hudson-river group. P. Portage group and Genesee slate.
H. Grey sandstone and Oneida conglomerate. R. Chemung group.
I, Medina sandstone. S. Old Red system. -
K. Clinton group. T. Conglomerate of the Carboniferous system.
a. Lake Ontario.
The distance upon the north side of the lake has been much shortened in proportion, in order to give more room for the
rocks upon the South side.
The same order of succession as here exhibited in the lower rocks and groups, may be seen
upon the northern shore of the lake between Gananoqui on the St. Lawrence, where the Pri-
mary and Potsdam sandstone are in juxtaposition, and Toronto, where the Hudson-river group
forms the only rock of the neighborhood. The Calciferous sandrock, Black-river and Trenton
limestones, are seen at intermediate points, covering extensive tracts in the neighborhood of
Kingston, Bay of Quinta, and other places. From the point where these rocks leave the
northern shore of the lake, they trend northwesterly; appearing upon the north side of Lake
Huron, and thence extending westward to the Mississippi river.
1. PotsDAM SANDSTONE.
The Potsdam sandstone is the lowest known sedimentary fossiliferous rock; it appears in
the Second district as a mass of great importance, and flanks the great Primary range OT
nucleus on the east, north and west, and rests directly upon the hard crystalline strata, as may
be seen by reference to the Geological map. It is usually of a pure quartzose character,
generally grey, though often striped, and sometimes partially or entirely red. From its proxi-
mity to rocks of igneous origin, it frequently assumes a slaty or gneissoid structure; and it
is not improbable that sometimes, in favorable situations, it becomes so completely disguised
as to be mistaken for a gneissoid or granular quartz rock. In places it appears as a conglo-
merate, but in all the localities examined on the north of Lake Ontario, the enclosed masses
are angular, showing them to be near their origin. This is an extensive rock, known as before
stated in New-York, Canada, and, from Dr. Houghton's researches, on Lake Superior; and
from position it is probably the same which appears on the Mississippi river, and mentioned
by Dr. Owen in his Report on the lead region of the northwest.
This rock is No. 1 of the Pennsylvania Survey, being common to that State, New-Jersey
28 GEOLOGY OF • THE FOURTH DISTRICT.
and Virginia. It is an interesting rock, as exhibiting to us the dawn of animal life; and the
first living thing entombed and preserved through unnumbered ages, its delicate structure un-
effaced to the present moment, is a species of Lingula, which is its only known fossil. This
fact affords a remarkable example of the tenacity of life in this family of shells, for we find
them in every successive group in the system; they have existed in every geological era, and
are living in the present Ocean. - -
2. CALCIFEROUS SANDROCK.
The Calciferous sandrock, a mass for the most part intermediate between sandstone and
limestone, being an intermixture of both, forms the next rock in succession, and appears
equally extensive. Indeed, in some places, it is more persistent than the former. It is a very
important rock in the First, Second and Third districts, both in extent and thickness. It is
likewise interesting from being the lowest position in which anthracite coal is known to exist,
being found in this rock associated with the quartz crystals. It yields the finest quartz crys-
tals known, and they are more or less abundant in all situations where the rock occurs.
Organic Remains. – In nearly all the situations where this rock appears, fossils are rare or
entirely wanting, and but few individuals have ever been found. Those at present known
are the following: Lingula acuminata, Ophileta levata, O. complanata, Pleurotomaria, Or-
thoceras primigenius, and plates of Crinoidea.
In the upper layers of this rock at Chazy, Dr. Emmons has obtained the following fossils:
Scalites angulatus, Maclurea labiatus, M. striatus, Bellerophon sulcatinus, Orthis and Orbi-
cula. - . -
There is also a layer characterized by the presence of fucoids, which is very persistent;
and probably from these marine plants is derived the carbonaceous matter which forms the
anthracite.
3. BLACK-RIVER LIMESTONE GROUP.
This group consisting of the Birdseye and Chazy limestone, is a remarkably persistent
mass, being known together with the succeeding one, almost or perhaps the entire width of
the continent. The rocks of this group appear in the northwestern part of New-York ; they
extend thence into Canada, and they are seen on Lake Huron, upon the Mississipppi river,
at Frankfort in Kentucky, and are well known in Pennsylvania and Virginia.
Organic Remains.—The Birdseye limestone of Prof. Eaton forms a part of this group,
being every where known by the presence of its peculiar fossil, the so called Fucoides demis-
sus, (since ascertained to be a coral,) which is typical of this rock in all situations. Besides
this fossil, it contains a species of trilobite, Orthoceras multicameratus, Ellipsolites ? Stro-
phomena laevis. Few others are known, and it usually appears destitute of such remains.
The Chazy limestone, which is considered by Dr. Emmons a distinct rock, contains a few
fossils peculiar to itself. These are the Maclurea, a fossil closely allied or identical to Euom-
phalus; Columnaria sulcata, with a few others.
LOWER ROCKS AND GROUPS. 29
4. TRENTon LIMESTONE.
This rock usually consists of a dark-colored limestone, intermixed and interlaminated with
black shaly matter of a character similar to the succeeding rock. It accompanies the Birdseye
in New-York, generally resting upon it in situations where both appear. In lithological cha-
racters and fossils, they differ essentially; the latter more particularly distinguish them. It
appears to be equally extensive with the mass below; the true distinction between them,
however, not being always observed.
Organic Remains.—This is geologically the lowest rock that yields an abundant harvest
to the palaeontologist. The following are already figured and described : Isotelus gigas, I.
planus, Bumastis trentonensis, Calymene Senaria, Calymene ! Illaenus trentonensis,
Ceraurus pleurexanthemus, Trinucleus tessellatus, Trocholites ammonius, Inachus undatus,
Pleurotomaria lenticularis" and three other undescribed species, Subulites elongata, Cyrtoceras
filosum, Cameroceras trentonensis, Orthoceras multilineatus, O. trentonensis and three other
undescribed species, Bellerophon punctifrons, B. bilobatus, B. profundus, Nucula inflata,
N. faba, Pterinea undata, P. orbicularis, Strophomena alternata, S. deltoidea, S. sericea,
Orthis striatula, O. pectinella, O. leptaenoides, Delthyris expansus, Delthyris ! Atrypa
extans, A. bisulcata, Favosites lycoperdon.
5. UTICA SLATE.
The Trenton limestone is succeeded by a dark or black carbonaceous slate. Where exten-
sive disturbances have prevailed, this mass is not every where distinguished from the group
which succeeds, though it merits a distinct place, from its general characters as well as from
its peculiar fossils. Within the State, it is every where black, and usually soft and fissile;
but from contained fossils, it would appear that its color has changed to green in Ohio and
other places at the west. Thin beds of impure limestone are associated with it in many
places. From a comparison of specimens from this rock when in the vicinity of hypogene or
altered masses, it corresponds very closely with the Llandeilo flags of Mr. Murchison; and
I have detected in specimens of the latter a small Lingula, which is very similar if not iden-
tical with one which occurs in the Utica slate. In its lithological characters, it does not differ
from the shale interlaminated with the Trenton limestone.
Organic Remains. – Triarthrus Beckii, Trocholites, Avicula insueta, Nucula poststriata,
N. Scitula, Cypricardia sinuata, Graptolites dentatus, G. Scalaris. The following are com-
mon to this rock and the Trenton limestone, according to Mr. Wanuxem : Orthis striatula,
Strophomena alternata, Lingula ovalis, Favosites lycoperdon, Isotelus gigas, Calymene
senaria.i • ... --
*--
* The Trochus lenticularis of the “Silurian System” 7 # See Report of Third District.
3{} GEOLOGY OF THE FOURTH DISTRICT,
$º
6. HUDson-RIVER GROUP.
Where the strata are undisturbed, a well marked line of division usually separates this group
from the Utica slate; but along the Hudson river, and in other places where disturbance has
prevailed, the two are not easily separable. Indeed from the fact that several fossils of the
Trenton rocks are continued through the Utica slate, and appear in this group, we might al-
most be inclined to consider it as a continuation of the same; beginning with a shaly limestone,
and passing through shale and shaly sandstone to the termination of the series. The group
consists of shales and shaly sandstones, with thin courses of limestone, and in many places
its upper portions abound in fossils.
Organic Remains.—The following are those enumerated and described : f Calymene
senaria! Triarthrus Beckii, Trinucleus caractaci, Avicula demissa, Pterinea carinata, Cypri-
cardia modiolaris, C. angustifrons, C. ovata, Nucula, Strophomena nasuta, f S. sericea,
Strophomena ! i Orthis striatula, O. Actoniae, O. testudinaria O. crispata, Orthoceras
aequalis, Pleurotomaria, stems of Crinoidea, Graptolites serratus, G. scalaris, &c. It will
be seen that several species (i) are common to this group and the Trenton limestone.
This group appears to be equally extensive with any of the lower masses, but its lithological
characters change essentially at distant localities. Upon the Hudson river, and in most other
places in New-York, it is exhibited in the form of slates and thin-bedded shaly sandstones,
forming what has been known as argillite and greywacke. Pursuing this group westward, it
is found in Ohio represented by limestone and shale or marl, forming the “Blue limestone” of
the Geological Reports of that State. It presents the same character in Kentucky, Indiana
and Wisconsin. At the same time, however, it retains many of its characteristic fossils, with
the addition of many new ones, or species which do not exist in any group in New-York.
This group thus exhibits an example where lithological character has ceased to be of any great
importance in identifying strata. The fossils at the same time are found to be much more
constant, though the greater number of individuals of different species renders the eastern
types less prominent than otherwise. -
This group not only extends into Canada on the north and east, but far west and southwest;
appearing, if we may judge from specimens, in Tennessee, and near the Hot Springs in
Arkansas. It is likewise an important rock in Pennsylvania and Virginia. This mass be-
comes interesting from the fact that it appears to be equivalent to the second great group in
the Silurian system of England, representing in its undisturbed and fossiliferous condition
the Caradoc sandstone. This would appear from the comparison of numerous specimens,
brought out by Mr. Lyell from well known localities in England, and which are now in the
Collection of the Lowell Institute at Boston. These leave no doubt of the perfect identity
in fossil and lithological characters. The same group, when disturbed and upheaved, as it is
on the Hudson river, doubtless represent the Cambrian system ; this portion having generally
been considered as a much older series than the same farther west. But the facts correspond
to those observed in England, viz. an identity in the contained fossils; the only difference
being produced by disturbance, and sometimes a partial alteration of the products.
LOWER ROCKS AND GROUPS, 3]
The change in organic remains at the termination of this group is very great, scarcely one
of the same species being known to exist in the higher rocks. It thus becomes an important
point, and well entitled to be considered as the line of division between the lower and higher
portions of this great system. -
7 & 8. ONEIDA ConglomERATE, AND GREY SANDSTONE.
In the eastern part of the State, the Hudson-river group is succeeded by a quartzose con-
glomerate; while in the western part, a grey sandstone occupies the same place. The con-
glomerate forms the Shawangunk mountain, and the mass in Oneida county and in Pennsylvania
attains a much greater thickness. It is not seen in place west of Oneida, though it appears
in boulders * scattered upon the surface. The Grey sandstone succeeds the Hudson-river
group in Oswego county, there being a gradual passage from the one to the other. It is in
character a grey quartzose sandstone, fine grained and compact, entirely destitute of fossils
except a few fucoids, thus forming a contrast with the mass below. -
Passing upward, the Grey sandstone intermingles with the Medina sandstone, which in its
lower part differs from that, chiefly in color, but its upper part contains peculiar fossils. The
red color of the Medina sandstone seems in some places to be partially communicated to the grey
below, which is often striped and spotted with red. There is lithologically no very strong line of
demarkation between the two rocks; thus offering a gradual passage from the Hudson-river
group to the Medina sandstone, which might perhaps with propriety be included in the lower
division. The chief difference is in color, and the occurrence of a few fossils not found below.
The latter rock forms the lowest mass of the Fourth district, and its connexion with those
below has been briefly explained; the short notices being intended merely for reference as to
order of succession, characters of strata and fossils; while for the details of each mass, the
other reports will be consulted.
The section shows the absence of three members: the “Grey sandstone,” the Hudson-
river group, and Utica slate. The whole width of the lake from the Genesee river northward,
is excavated in the lower part of the Medina sandstone, and the whole of the three groups
enumerated. Farther west along the southern shore of the lake, pebbles and worn fragments
of the rocks of the Hudson-river group, containing the common fossils, occur in great num-
bers. 4.
To the south of the lake, the section exhibits the rocks of the New-York System, from the
Medina sandstone upwards, in their order of succession, and also their connexion with the next
higher masses. In this order, the different rocks and groups will follow in the succeeding
chapters.
* See Report of Third District: Oneida conglomerate.
32 GEOLOGY OF THE FOURTH DISTRICT,
CHAPTER. W.
Description of the rocks and groups of the New-York System embraced within the
- , Fourth Geological District. - -
The previous chapter contains an enumeration of the deposits forming that part of the
New-York System between the Primary and the Medina sandstone, or No. 9 in the order of
succession, and the lowest rock of the district. The rocks of the Fourth district consist prin-
cipally of series of limestones, shales and sandstones, each passing into the other by insen-
sible gradations in some points, while in others the line of separation is distinctly marked.
Each formation or stratum is limited on the north by its outcrop, and on the south by the
superposition of the next successive deposit, under which it disappears. These are for the
most part continuations of those which commence farther east. In some instances they have
thinned partially, and some members of the Helderberg series are wanting; in others, as the
Medina sandstone, and Niagara group, the greatest development appears within the limits of
this district, and diminishes to the east.
Investigations throughout the whole State have proved that there is some one point or
limited area where each rock, or the members of each group, are better developed than in any
other, and this one is adopted for the name. The advantage of names from localities over
those from descriptive characters, is decidedly great. In the latter case, the description or
character may not convey to the reader precisely the same ideas as those possessed by the
writer; and again, distinctions in character cannot be so accurately described, but that another
rock may possess the same in a sufficient degree to be mistaken for the true one. The charac-
ters of a rock rarely remain uniform over a great extent of country; and hence a descriptive
name, applicable in one place, may not be so in another. On the other hand, when a name is
given from the locality, the description of the rock follows; and although it may vary at distant
points, or another rock be found possessing the same character, still the type remains; and
whatever of doubt or obscurity may ever arise, the examination of the original locality would
decide all difficulties. Since rocks are identified more by their fossil contents than by their
lithological character, a name descriptive of the latter is of less consequence than formerly,
when fossils were the subordinate characters of a mass.
Notwithstanding, however, that palaeontological characters have taken precedence over all -
others in distinguishing sedimentary strata, still the lithological character must not be over-
looked; for in some cases it will be found an unerring guide, if properly understood, ove"
LOWER ROCKS AND GROUPS. 33
t
*
#
¥.
hundreds of miles in extent. Changes in the lithological features of a rock, also, which may
render observations unsatisfactory or doubtful, are usually accompanied by greater or less
change in the nature of the fossils. In no case, therefore, are to be overlooked either of the
three important facts and characters, viz. Lithological character, order of superposition, and
the nature of the contained fossils. A more extended knowledge of the development of the
great groups of the older sedimentary deposits, which with some exceptions or interruptions
extend almost across the continent, will enable us to appreciate more fully the comparative
importance of the distinctive characters by which they are identified.
GEOL, 4TH DIST. 5
34 GEOLOGY OF THE FOURTH DISTRICT,
§§
sº §§ ()
W ºš NS š @Nº.
w §§
§
§§
- §§§
§§ [] §
lº W S
º §§ §§§§
Ş §§ º
§
&S$ º
ºWºRSºS
§§§ º
§§ º §§§ SN
Sºrºs Rºnsº
§§§§ Nºš
§§§ § N º N §§ º §
§§ §§§
§§§ §§§
（iii); #: -
iſſiº
| º |||}|
º;
|; º
;
... *.*, *, * *-*.
-_ - "...- ... :: ->
:..-e-ºs:
--> -
--
View of Medina Falls, from a Sketch by Mrs. HALL.
9. MEDINA SANDSTONE.
Saliferous rock, of Eaton; Niagara sandstone, Red sandstone of Oswego, Variegated
sandstone, and Red marl and sandstone, of the Annual Reports.
(No. 5, of PENNsyLVANIA SURVEY.)
This mass is usually a red or slightly variegated sandstone, solid and coherent in the eastern
extremity of the district, becoming friable and marly in its western extension, and admitting
an intercalated mass of grey quartzose sandstone which contains marine shells; while in the red
portions, are rarely found other than marine vegetables or fucoids. This rock gives origin to
brine springs throughout its whole range. It extends westward beyond the limits of the
district into Canada, but is not known in the southwest, in Ohio and Indiana. Both in Penn-
sylvania and Virginia, it is found possessing the same essential characters as in New-York.
The locality which gives the name, exhibits the rock best developed, and with its charac-
teristic fossils. The rock is the lowest of the district, and the ninth of the New-York System
in the ascending order. -
By reference to the Geological map of the State, it will be seen that this rock extends
throughout the district from east to west, bordering Lake Ontario. It forms but a narrow
band in Wayne county, but expands to the westward, and seems to attain its greatest thick-
ness near the Niagara river; as is indicated by the breadth of surface occupied by the mass,
MEDINA SANDSTONE, 35
->
and also from the fact that it appears on the north side of the lake to the west of Toronto.
It continues beyond the Niagara river, having been traced as far as the head of Lake Ontario,
and it is believed to extend much farther westward. .
In Wayne county, it is usually a firm siliceous rock, approaching to a conglomerate in some
places near the lake level. On going westward, the sand in part gives place to argillaceous
matter; and before reaching the Genesee, the greater part of the mass, visible above the lake,
has become a marly sandstone; the upper part, only, being firm, and withstanding the effects
of weathering. Its enduring character in the eastern part of the district is well exhibited by
the great number of pebbles and boulders scattered over the surface of Wayne county, and
some parts of Monroe, and which diminish westward. Pebbles of this rock, however, form
a large portion of the drift far to the south, and may be found intermingled with the products
of more southern ranges, in all the valleys as far as the Pennsylvania line. In some places
in the northern range of counties of the district, the surface is literally covered with pebbles
of this rock, almost wholly unmixed with any other. -
From its shaly or marly character upon the Genesee river and in the country west, this rock
was originally mistaken for the red shale of the Salt group, which it closely resembles. The
latter appears in Onondaga county on the canal; and by following the same line westward,
no other rock appears until within a short distance of Rochester. The marly sandstone ap-
pearing here was naturally taken for a continuation of the rock seen in the vicinity of Syracuse,
and the occurrence of salt springs likewise aided to complete the deception. This opinion
prevailed until the Geological survey had made some progress, when it was found that the
Clinton and Niagara groups both intervened between the Medina sandstone and the continua-
tion of the Onondaga-salt group.
The scenery exhibited along the line of outcrop of this rock is in some places interesting in
the highest degree. In Wayne county, from its rising but little above the lake, it forms only
some inconsiderable falls in the streams; always strongly contrasting, by its deep reddish
brown color, with the rocks above. In Monroe county, it forms the lower falls of the Gene-
see, one hundred, and ten feet in height; one of the most picturesque spots in the district,
exhibiting not only this rock, but above it, in the cliff, the Clinton group and shale of the Nia-
gara. It also forms the banks of the river below, extending nearly to the lake. In Orleans
county, at Albion, there is a low fall on Sandy creek over the same sandstone; and by fol-
lowing that stream farther up, its connection with the higher rocks can be readily observed.
At Medina, on Oak-orchard creek, this rock forms the beautiful little cascade represented in
the woodcut. - - -
The deep gorge and the high cliffs on either side of the Niagara at Lewiston, are more than
half excavated in this rock; and the partial obstruction of the water at the whirlpool is caused
by a part of the same mass. Its alternations of harder and softer masses produce cliffs or
cascades along its whole extent. - - .
This rock, where best developed, admits of a fourfold division, as it appears throughout the
greater part of the Fourth district. Including the “Grey band,” which here forms an integral
part of the mass, it may be represented as follows: -
36 GEOLOGY OF THE FOURTH DISTRICT.
1. Red marl, and marly or shaly sandstone, sometimes banded and spotted with green; the bands hori.
Zontal, or parallel to the strata, and vertical.
2. Grey quartzose sandstone, entirely distinct from the mass below. -
3. The lower part is merely a repetition of No. 1; gradually passing into a more Sandy form in the
western portion of the district, while in the eastern portion the whole of this division is more
siliceous, the central mass (No. 2) not appearing.
4. The grey or greenish grey terminal portion of the mass, which in the Third district is considered
a distinct rock, forming the Oneida or Shawangunk conglomerate. In the Fourth district, it
always appears more or less as a part of the Medina sandstone, possessing the same lithological
features.
1. RED MARLY OR SHALY SANDSTONE.
Throughout the counties of Niagara, Orleans and Monroe, the lower part of this rock is a
soft red shale or marl, with but a small admixture of siliceous matter. It coheres but slightly
where weathered, and readily decomposes to a loamy clay. When exposed in the banks of
ravines and streams, it presents a cracked and crumbling appearance; the surface crossed in
every direction by seams, separating the whole into small angular fragments, which are con-
stantly softened and detached by the weather, exposing a fresh surface which in turn undergoes
the like changes. The first appearance, after being broken down in this manner, is that of
cubical or angular fragments, which are easily crushed in the hand, mixed with a smaller
proportion of soft clay. The process of disintegration goes on till the whole is reduced to a
clayey soil of a brick-red or brownish color. These changes may be witnessed on the banks
of the Niagara at Lewiston, the banks of the Genesee below Rochester landing, and in nearly
all the small streams crossing the Ridge road between the Genesee and Niagara rivers.
In Wayne county, the lower division of this rock can scarcely be said to exist, though that
portion near the level of the lake possesses in a considerable degree the same characters. The
color of the decomposing rock has been communicated, often in a high degree, to the soil above.
This is more particularly seen where the covering of transported materials is light, as through-
out all that portion of the country between the Ridge road and Lake Ontario. The same color
prevails in a less degree, much farther south, where the materials derived from the destruction
of this rock form a large proportion of the drift or transported matter, producing the soil of the
district. This brownish color of the soil will not be confounded with the deep red color pro-
duced by the destruction of the red shale of the Onondaga-salt group, which is seen to a great
extent farther east, but which has had little influence in the Fourth district.
The uniform texture of this part of the rock, is the cause of the very even surface of the
country bordering Lake Ontario between the Genesee and Niagara rivers. The same cha-
racter is presented in some degree east of the Genesee, except where interrupted by hills of
drift. When penetrated to some distance, it appears compact, and is readily quarried into
large blocks, but it does not withstand the effects of weathering. This has been tested by the
experience of many years; and the quarries in this division of the rock are now, I believe,
generally abandoned. -
MEDINA SANDSTONE, - 37
This is one of the most uniform masses in the whole district, the only change in its whole
extent being the gradual increase of argillaceous matter in a westerly direction. Its uniform
reddish brown color is but slightly relieved by the occasional spots and bands of green, and
the absence of fossils renders it a very uninteresting rock to the geological observer.
2. GREY QUARTzos.E SANDSTONE.
In the western part of the district, the lower division is succeeded by a grey quartzose
sandstone, exhibiting a sudden contrast in the material and coloring matter. This mass, which
is twenty-five feet thick on the Niagara river, extends through Niagara and Orleans counties,
but is not seen in Monroe or Wayne, either from having thinned out, or from passing beneath
the lake; the former is more probable, as there is no evidence of the latter. From Medina
westward it exhibits a prominent line, rising abruptly from the softer rocks below, and jutting
out beyond those above, forming a terrace, which runs a little to the north of the great lime-
stone terrace or mountain ridge. It appears as a projecting band in the banks of the Niagara
river, extending from Lewiston as far as the Whirlpool, where it disappears beneath the level
of the water. - -
The mass is mostly composed of thin layers, from the thickness of one-eighth of an inch to
six inches. Near the Niagara river the layers are generally thicker, the deposition apparently
having been more rapid. At a quarry one mile north of Lockport, the layers are often ex-
ceedingly thin, not more than one-eighth to one-fourth of an inch, and perfectly separable from
each other, the planes in many instances presenting a partial coating of the oxide of manganese.
The surfaces are exceedingly smooth, as if washed by water before the deposition of the suc-
ceeding layers; in other cases they are covered with the separated valves of Lingula, and
marked with numerous wave-lines. - - . .
This mass, which is light grey or nearly white on the Niagara river, becomes slightly tinged
with red on going eastward, and at Medina some thin layers are strongly colored; it, how-
ever, maintains its general uniformity, the grey color and quartzose character every where
predominating. East of Medina it is seen in but few places, and in these not well developed.
In lithological character, this mass bears a very close analogy to the sandstone forming the
terminal member of the Clinton group in Herkimer county, as it appears on the south side of
the Mohawk in several places. The peculiar fossils are wanting, however, and the association
is entirely unlike. -
The range of the grey sandstone from Lewiston eastward is, for several miles along the base
of the escarpment, formed by the Niagara limestone; afterwards it extends a little farther
northward, and becomes from thence a distinct elevation from half a mile to one mile north of
the principal terrace, and nearly parallel with it. The descent over its outcropping edge is
a rapid slope, covered with fragments of the sandstone broken up and mingled with the soil.
After passing a few miles to the east of Lockport, the elevation produced by this rock merges
in the general level of the country; and thence eastward, exhibits upon the surface no evidence
{ .
*
of its existence.
38 GEOLOGY OF THE FOURTH DISTRICT.
This rock is extensively quarried for flagging stones a mile north of Lockport, where slabs
of the finest quality, and of any dimensions, are obtained. The surfaces are almost entirely
smooth, interrupted only by the slight wave-lines; they can be obtained of any desirable thick-
ness, and from their uniform quartzose character, are extremely durable, and wear evenly.
These quarries are owned by Whitmore & Co.
Some quarries in this rock have more recently been opened near Medina, where stone of
similar character is obtained; and when a sufficient demand for the article shall be created,
the whole distance from Medina to Lockport, along the outcrop, can be converted to an open
quarry. At Lewiston, where the rock has been excavated, it does not furnish so good flagging
stones, the layers being thicker, and better suited for building. Other localities in the neigh-
borhood may, however, prove of a different character.
3. RED SHALE AND SANDSTONE.
The grey quartzose sandstone is succeeded by a red shaly or marly mass, similar to that
below, which soon alternates with thin courses of red argillaceous or quartzose sandstone.
The shaly matter diminishes, and the sandstone increases in the same ratio as we ascend, and
towards the top becomes mingled with grey or greenish grey in large proportion. The whole
is finally terminated by a grey or ash-colored siliceous, or, in some places, argillaceous sand-
stone, differing but slightly from that below.
This division of the rock is mottled or variegated with spots and lines of grey and green;
these are often circular, presenting the same structure and composition as the mass around.
The difference of color is owing to a change in the oxidation of the iron, which is the coloring
principle of the rock, and has been produced by some carbonaceous or bituminous substance
lodged at a point now the centre of the green spot. Bands of green, parallel to the stratification,
have been produced in the same manner, the carbonaceous matter spreading over a considerable
surface. Lines of green perpendicular to the stratification, which frequently occur, are not
so readily explained upon any supposition of this kind, and I am inclined to believe that they
have been produced by the infiltration of water charged with carbonaceous matter from the
soil above. That water may produce such discoloration, I have observed many facts to cor-
roborate; and if the change in color can be produced by a small quantity of bituminous or
carbonaceous matter, for some distance around it, I see no reason why the same change may
not be produced by water flowing through peaty soils, and passing into a seam or joint in the
rock. I have seen pebbles of the same red rock of the more sandy variety, which had lain in
the bed of a muck swamp, with the color completely discharged from the outer part. The
color is likewise lost by continued heat, as is proved in stones used in the furnace at Wolcott.
The presence of carbon, in this instance, may have aided to produce the change.
MEDINA SANDSTONE, . 39
4. GREENISH GREY ARGILLAGEOUS oR SILICEous SANDSTONE. Grey Band of EATON.
Towards the upper part of the Third division, the coloring matter becomes less universally
diffused, or the deoxidizing process has been more efficient, and spots and lines of grey in-
crease until the greater part becomes of that color. At this stage there is sometimes an
increase of argillaceous, at others of siliceous matter, and a gradual passage into the upper
division of the rock. At Lockport, and in some parts of Wayne county, this part of the rock
is a green marl with spots of bright green shale intermixed. It is generally argillaceous in
character, though at Lewiston some portions are highly siliceous. The variation from the
mass below is chiefly in color, and it forms a marked line, contrasting strongly with the dark
brick-red of the Third division. The intimate connexion of this portion with that below pre-
cludes the idea of considering it a distinct rock, as color is the chief difference; and this change,
though often abrupt, is usually gradual. It sometimes contains small black pebbles, which
appear at first view like organic bodies, but they are never in sufficient proportion to give
it the appearance of a conglomerate. These may be seen at Medina, and at Lewiston, spa-
ringly scattered through the rock, differing entirely in character from the surrounding mass.
This division of the rock is very variable in thickness, and in some places scarcely recogniza-
ble. In the eastern part of Wayne county it is about three feet thick, at another locality but a
few inches; on the Genesee river it is nearly five feet, at Medina about four feet, at Lockport
less than two feet, and on the Niagara river it is ten feet thick.
The intercalation of the grey siliceous mass (No. 2), differing in color and lithological cha-
racters, and the repetition above of precisely the same products as below, reveals a fact of
great interest, showing that important changes occurred in the condition of the deposits during
what we regard as a single period. After a long continued deposition of the mud formation
highly colored by oxide of iron, there was an entire cessation so far as to allow the deposition
of uncolored or grey and purely quartzose sandstone; after which, the former red deposit was
resumed precisely as below. All the circumstances connected with this quartzose deposit
are interesting, it being the only part of the rock where animal organic remains are found.
Here we find Lingula, Cytherina and Pleurotomaria in great numbers, besides Bellerophon,
Cypricardia and Orthoceras in less profusion. The condition of all these fossils, however,
indicates disturbance in the waters from which the mass was deposited, or rather near the
close of its deposition. The Lingulae, so far as ascertained, are all of broken or single valves,
and usually crowded together in great confusion; the other fossils present the same appearance -
of having been drifted into their present situation. At Medina, these fossils are near the
upper part of the grey mass, and are not found above; they are here more abundant than in
any other place, few being seen west of Lockport. The cause of this agglomeration and
destruction may perhaps be explained by changes which took place in the condition of the
mass during its deposition, as indicated by appearances near Lockport and elsewhere. These
conditions seem to have been either the frequent oscillation of the surface; or that the mass
in which they are imbedded formed at that time a sandy beach, over which the tide sometimes
40 GEOLOGY OF THE FOURTH DISTRICT.
quietly ebbed and flowed, and where again the stormy waves dashed with fury, destroying
and overwhelming all within their reach. - - -
If we might be allowed to hazard a conjecture as to the changes and their causes going on
at the time of the deposition of these different divisions, we would incline to the belief, that
the lower shaly deposit was the product of a mud volcano, rapidly ejected and spread over
the surface, rendering the sea turbid and discolored to such a degree as to prevent the exis-
tence of any organic forms." Afterwards a cessation of the volcanic action allowed the depo- .
sition of the grey quartzose mass; the materials having, perhaps, the same origin as the grey
sandstone which was formed previous to the commencement of the Medina. Although during
this period there was no matter ejected from the volcano, still it may have produced oscilla-
tions of the surface, causing alternate deep and shallow water, or deep water in some places
and shallow in others. Subsequently, towards the close of the grey deposit, the volcano
broke forth again, with renewed energy, destroying all the organic forms which had come into
existence during this comparatively quiescent period, and overwhelming the whole with
another deposit of red mud like that below. Again after a time, the subterranean action ap-
pears to have become more quiet, gradually subsiding, and allowing an increase of sandy
matter from some other source. Lastly, toward the termination of the deposit of mud, and
when the sand had increased considerably, we find an abundance of the vegetable forms given
in the woodcut and plate, and the whole series terminating with the grey division, marked by
that singular fossil the Dictuolites.
Diagonal lamination.—The sandy strata at Rochester, Medina and elsewhere, exhibit dia-
gonal lines of deposition; and in some places these lines are more strongly marked than those
of the stratification, and the rock presents the appearance of being inclined.
* The fragments of fucoids found may have been drifted from some distant locality.
MEDINA SANDSTONE. - 41
The above woodcut will give an idea of this appearance; in other instances the lines are
more curved, though generally when seen on a large scale, they are nearly straight. From
the interlamination of shaly matter, the strata to which this structure is confined often appear
in wedge-form layers of greater or less extent, enclosed between parallel lines. In most in-
stances this structure is clearly produced by deposition alone; but where the lines of lamina-
- 4. tion, as indicated by color, are strongly curved as in the wood-
- cut No. 4, it seems impossible that it could have been produced
by deposition. As this rock is everywhere free from distur-
bances or upliftings, there could have been no lateral move-
ment, except on a small scale, to have produced this effect.
The infiltration of finer particles, with a greater proportion of
coloring matter, may perhaps explain the appearance without
having recourse to any extraneous agency. This structure is
seen in the more siliceous strata on the Genesee below the
- º lower falls, and at Medina. -
In many places where this diagonal lamination is exhibited, there is a tendency to the pro-
duction of conglomerate in the associated strata. Thin layers of pebbles and angular frag-
ments are of frequent occurrence at Rochester, Medina and other places, and associated with
them and the more sandy portions of the rock, are frequently found fragments of what appear
to be shells of Lingula. The latter may be seen in loose specimens somewhat weathered,
below the lower falls of the Genesee, at Rochester.
In specimens which I have more recently collected, the fragments of shells appear as if
drifted by waves and spread evenly over the surface, precisely in the same manner as com-
minuted shells upon the shore of the ocean. In instances of this kind, after walking for a
mile upon a sandy beach, without seeing anything other than a stranded Fucus, I have sud-
denly come upon a space several feet in extent, which, apparently from a slight eddy, or
inequality in the surface, was covered with comminuted shells and fragments of coral. The
analogy to some of our sandstones where organic remains are rare, is thus most strikingly
exhibited. -
Accretions.—In the Second division of this rock, at Lewiston, and other places, we notice.
upon the surface small points and blotches of fine black sand, scarcely cohering, and which
crumbles on the touch. These in many places are larger; and at Lockport, in the thin-bedded
sandstone, they are frequently several inches in diameter. All have the same incoherent
structure, appearing like a mass of black or dark colored sand, around which the strata have
been deposited. From the manner of their occurrence, and from the stratum frequently being
a little elevated just around them, it is evident that they were formed during the deposition of
the mass. Their limits are well defined, and they separate from the stratum, frequently leav-
ing a circular hole in the quarried slab. A specimen of this kind may be seen in the State
Collection. In a few instances I have observed these masses of black sand surrounded by a
firm coating or shell of sandstone an inch thick, like the ordinary rock, but separating from
the stratum, and presenting a smooth spheroid. This peculiar form of accretion I have seen
GEoL. 4TH DIST. 6
42 GEOLOGY OF THE FOURTH DISTRICT.
only in this rock; the structure is quite unlike the bodies of this kind usually met with, and
seems due to the decomposition of iron pyrites, or some other substance where the force was
directed outwards, rather than toward the centre. -
The sandy portions of the Third division often contain oblong or rounded accretions or peb-
bles of shale, which on weathering are dissolved out, and leave corresponding cavities. These
appear much like worn fragments of the red shaly part of the rock, and are distinctly lami-
nated; still from the manner of their being imbedded, and uniform size, they are probably
referable to the first named cause. They are always of a deep reddish brown, while the mass
which contains them is frequently much lighter in color. This, if they were contemporaneous,
only shows the superior attraction of the argillaceous mud, for the coloring matter, over the
sandy portions of the rock. The flattened oblong form of many, renders it a matter of doubt
whether they are accretions or pebbles.
Localities. – This rock appears as a conglomerate in a ravine near the level of the lake,
about two miles northeast of Wolcott furnace. This was the farthest eastern point at which
it could be detected in the district. An examination was made for this rock from the Wolcott
ore bed towards the lake, but without success, the low marshy ground preventing its appear-
ance. The same is true at Wolcott furnace, and also on the west side of Little Sodus bay.
The sandstone is quarried on Beard's creek and Little Red creek in the town of Wolcott,
and used in the construction of furnaces. It is again well exposed near the forge on Salmon
creek, and contains its characteristic fossil, the Fucoides Harlani. It also appears in the
town of Williamson, near the lake shore. -
In Monroe county, in the town of Penfield, this sandstone appears on the lake shore, pre-
senting a few feet of the strata below the clay and gravel. On the eastern side of Irondequoit
bay, it has been quarried for the piers at the mouth of the Genesee. It appears again near
the head of the bay. - - - -
The lower falls of the Genesee are caused by this rock, more than one hundred feet being
exposed at that place. From the falls it forms both banks of the river, extending nearly to
the lake. This is one of the best localities in the district. It is again seen a little north of
Adams's basin, about twelve miles west of Rochester. In passing through Sweden, about
twenty miles west of Rochester, the bed of the canal was excavated in this rock.
West of the Genesee the sandstone does not appear on the lake shore in Monroe county,
but by tracing up the small streams it may always be found; it is of little interest, however,
from its uniform character and the absence of fossils. A short distance northwest of Adams's
basin, the rock with Fucoides Harlani appears in the bed of a small stream. In the neighbor-
hood of Clarkson corners, it approaches the surface, giving its characteristic color to the soil.
The upper part of the mass, abounding in the Fucoides Harlani, is quarried near the village
of Brockport; and also in the northern part of Clarendon, Orleans county, forming a good and
durable building and flagging stone. The softer portions are well developed in the banks of
Sandy creek, particularly at the crossing of the Ridge road, and also nearer to the lake.
MEDINA SANDSTONE. 43
The rock again appears near Holley, and at numerous places on the Erie canal westward.
It is well exposed in the small stream on the south side of the canal near Albion, and is seen
more or less between this place and Medina.
At Medina, on the Oak-orchard creek, we have the best exposure of the mass, which exists
in the State, and hence its name. The thickness here exposed is not greater than on the
Genesee river, nor so great as on the Niagara at Lewiston, but it exhibits all its fossil types
in the greatest perfection.
A little northwest of the village, it is quarried for flagging stones. From Medina westward
it is almost constantly to be observed either in the canal, or in the terrace formed by the out-
cropping edge of the middle division as far as Lockport. At this place it is well exposed
about a mile below the village, on Eighteen-mile creek, exhibiting likewise its fossil shells,
though in less profusion than at Medina. The Fucoides Harlani, however, is rare, and not
well preserved here. In the quarries, and the brow of the hill further north, the central portion
of the mass is well exposed. | . .
From Lockport westward, the Third and Fourth divisions form part of the slope of the
terrace, contributing to the height of the same above the country on the north. The central
hard portion being less destructible, has protected the base of the terrace, and projects be-
yond the higher part in a step or table. , º
In the banks of the Niagara, it is very finely exposed. At Lewiston, it exhibits about two
hundred feet in thickness, and gradually declining, passes beneath the water before reaching
the falls. The grey quartzose sandstone, like that at Lockport and Medina, is seen at the
Whirlpool, projecting into the river on either side, and forming a barrier which has at one
period obstructed the waters in their passage to the lake. Below Lewiston it is seen in the
banks of the river, extending nearly to the lake shore, where it slopes down, and becomes
covered by the superincumbent clay. - -
On the Welland canal, at St. Catharines, at Hamilton, and numerous other places along
the slope of the terrace, this rock may be seen, showing its continuation beyond New-York,
and in the same line of direction.
Thickness. – From the circumstance that the base of this rock is nowhere to be seen in
the Fourth district, its entire thickness cannot be ascertained. Its greatest width is on the
Niagara river; but here a large portion of it is excavated on the north, leaving probably less
than half its original extent within the State. From the width here exposed, the thickness
actually measured, and the rate of dip to the southward, there is about three hundred and fifty
feet of the rock between the mouth of Niagara river and the termination of the rock above
Lewiston. By reference to the Geological map, it will be seen that this rock thins out en-
tirely in an easterly direction in Oneida county; showing from that point westerly as far as
Lake Ontario, a gradual increase in thickness. Examinations farther westward are required
before the point of its greatest development can be ascertained. -
44 GEOLOGY OF THE FOURTH DISTRICT.
Mineral Contents of the Rock.
Copper and iron pyrites, with oxide of manganese and iron, and carbonate of copper, are
the only metallic substances I have met with in this rock, and these only in minute quantities.
At Lewiston the upper part of the mass contains numerous small spiculae of pyritous copper,
and the fissures and joints are often lined with a thin coating of green carbonate of copper; and
on subsequent examination, I find that at this locality it is very generally diffused, though the
quantity is small. - -
The hydrated peroxide of iron is seen lining small cavities in the grey quartzose sandstone
at Lewiston and elsewhere; and the black oxide of manganese is commonly seen in the joints
and between the laminae, though never in large quantities.
A reddish colored sulphate of baryta in small spherical masses, or filling small cavities in
the rock, occurs at Rochester and a few other places. -
Carburetted hydrogen gas rises from this rock in considerable abundance in some places
along the Erie canal east of Lockport. The principal point is Gasport, where it is collected
and passed through a tube, supplying a quantity sufficient to illuminate a large room constant-
ly. The light is less brilliant than that of artificial gas, being more yellow, and, from the
manner in which it is consumed, giving rise to much smoke. I have seen no places which
emit sufficient quantity to induce the erection of apparatus for collecting it, except as a matter
of curiosity. The evidence of bituminous matter is here fully established, even if the green
threads and spots were not considered sufficient; but the origin of this is still left in obscurity.
The amount of organic matter, both animal and vegetable, known in this rock, is so exceed-
ingly small, that it could scarcely be supposed to give rise to the constant emission of this
gas. The impervious nature of the lower part of the mass, and the absence of fossils in the
next rock below, would preclude the idea of its origin in that direction, as there are no dis-
turbances known in the district. - -
Springs.-Along the outcropping edges of the siliceous portions of the mass the soil is
thin, and water readily percolates through the fissures, offering no springs. The more even
surfaces, particularly of the lower division, are sufficiently moist, and in level situations or
depressions too much so, for fertility. Springs are of frequent occurrence at the junction of
the Second division with the more impervious mass below.
Saline springs are everywhere to be found in this rock throughout its whole extent, from
the eastern part of Wayne county, and even as far as Oswego, to the Niagara river; and
beyond this, in Canada, deep borings have been made and much salt water obtained. In
some places salt had been manufactured for a long time previous to opening the Erie canal;
but the greater facilities and better quality of the brine at Salina, with that means of transpor-
tation, soon superseded the manufacture of salt from any of the springs in this rock. It ap-
pears in all cases where I have been able to obtain any knowledge upon the subject, that there
is a large admixture of impurity in the brine, and the salt has a “sharp bitter taste” and brown
MEDINA SANDSTONE, 45
color: the taste owing probably to muriate of lime and the color to iron. This objection could
probably have been obviated, had the strength and quantity of the brine been sufficient to war-
rant the undertaking. - -
There were never, so far as I have learned, very extensive operations carried on at these
brine springs. The borings have rarely been made to any great depth, and the quantity of
water being small, the fixtures have been temporary, and, from disuse, nearly every spring
visited had become filled with fresh water. In a few cases the destruction of vegetation
around, and the saline taste of the earth, fully indicate the presence of salt.
I have not been able to satisfy myself that deeper boring was always attended with an in-
crease in the strength of the brine, though in a few cases this has been recorded as the fact.
At St. Catharines, U. C., where a boring of five hundred feet was made in this rock, I was
informed that the strength of brine increased with the depth; but here, as well as elsewhere,
the work has been abandoned.”
From the situation of numerous springs of this kind which I visited, and which are upon
level ground, or in depressions having little or no outlet, I am disposed to believe that a depres-
sion in the rock, with the exposure of much surface, concentrating its saline matter in one
point, is required for their production. In the greater number known to me, the discovery
was made by the saline water rising to the surface, but in many instances it was found by
excavating or boring into the rock in places where no salt spring was previously known; and
in almost all cases where excavations have been made in the lower division of this mass, the
water is more or less brackish. From these facts we have almost conclusive evidence that
this deposit, throughout its whole extent, is impregnated by Saline matter. 4.
A fact of this kind has lately come to my knowledge, through Judge Allen of Saratoga.
During the extreme drought of the summer of 1841, the wells situated upon this rock in many
towns in Orleans county became dry, and they were in consequence excavated or bored to a
greater depth; and in nearly all cases the water proved to be in some degree saline, and in one
case so much so as to warrant the erection of fixtures for the manufacture of salt. Most of
these wells were in situations where salt water had never before been known to exist, and
furnish another fact in evidence of the wide distribution of the saline ingredients.
Agricultural characters—The soil overlying this rock, from the varying nature of the mass
below, is of the same character. In the eastern part of the district it is a Sandy loam, or in
numerous instances sandy; the argillaceous nature of the rock increasing in a westerly direc-
tion has given rise, generally, to sandy loam. Limited tracts are sandy, and other portions
are again of a clayey nature. Whenever the rock approaches the surface, the soil is a heavy
mixture of clayey loam and fragmentary matter; proper cultivation, however, mollifies this
nature, and it is considered among the most fertile soils of the district. From the fact that
* I find the following record in my notes, made at St. Catharines. Depth of boring 500 feet. Water at 300 feet 27°; at 429
feet 29°, but this increase in specific gravity was not constant, and it is not certain that the water increased in strength on de-
scending.
46 GEOLOGY OF THE FOURTH DISTRICT.
Lake Ontario has recently occupied all that part of the district north of the Ridge road, the
soil is not as evenly distributed or as uniform in character as it otherwise would have been.
Slight elevations of sand, or sandbars, have accumulated in many places, and argillaceous ma-
terials at intervening points. The surface, therefore, presents all varieties from a light sand
to a heavy clay loam, or gravelly loam. The drifted materials which occupy a considerable
portion of the surface in Wayne county, are mostly of loose gravel and sand.
Organic Remains of the Medina Sandstone.
In this rock, like all others colored by the red oxide of iron, fossils are rare, and through-
out the greater part of the first and third divisions, the only fossil remains are Fucoides. In
the lower division few of these have been found; mostly in fragments, and in such a condi-
tion as would indicate their partial destruction before being imbedded, or their subsequent
absorption by the matter of the rock. The green threads and spots, probably due to some
organic nucleus, disclose nothing by which its nature can be ascertained, and we are left to
conjecture as to what may have been their origin.
In the third division of the rock two species of Fucoides abound in great perfection, the
F. Harlani and the F. auriformis. These are always attached to the under surfaces of the
layers, and rest upon a bed of shale, as if they had grown upon the clayey bottom, and been
buried by the first succeeding deposition of sand. The first named species is very abundant,
often covering with its beautiful articulated branches the surface for many feet in extent.
The other species is also abundant in many places.
#
-
§§
#j |%/)º
|
%
£3.2 º º
#3 %
º sº
|
iſſ
º
WS | º iń. sº
$ º
Figs, 1 and 2. Fucoides Harlani.
MEDINA SANDSTONE. 47
The Fucoides Harlani is everywhere typical of the Medina sandstone, continuing through-
out its whole extent so far as known. It occurs in the Third district, at Fulton, Oswego
county, and in the Fourth district in Wayne county, at Rochester, Medina, and on the Nia-
gara river. In Canada, it is found along the Welland canal, besides numerous intermediate
places. According to Mr. Vanuxem, it occurs in Pennsylvania and Virginia, having the same
association. It thus becomes the most characteristic indication of the rock, and is considered
as one of its essential organic forms, occurring in no other rock, and being an example of a
peculiar type which commenced and terminated its existence with this rock. The second
figure in the woodcut represents that part of the fossil near the base, from which the branches
diverge. Fig. 1 is a more common form, and the most abundant is that of single, elongated,
straight or curved branches, crossing each other in various directions upon the surface of the
stone. Their annular ridges or apparent articulations are always visible, except when much
weathered, and from these it was formerly supposed to be the stem of a crinoid. The sub-
stance of this fossil is frequently replaced by pebbles and small angular fragments, and in such
cases the beautiful annulated structure is less distinctly visible. The Fucoides auriformis
(Pl. I. fig. 2) is equally common in the Fourth district, it being abundant at Rochester, Medina,
and other places, holding the same position as the first. It appears slightly elevated above
the surface of the stone in the form represented in the figure, like a collection of small auri-
form appendages, whence it receives its name. -
The Fucoides heterophyllus (Pl. I. fig. 3) is allied to the preceding, and abounds at
Rochester. This figure will be readily recognized by any one who has explored the river
banks below the lower falls. The representation is of its more common form, but there are
many other varieties which may be referred to this species. Its great uniformity in general
appearance and manner of occurrence, indicates that it is organic ; and for the present all
forms of marine vegetation, which have no characters sufficiently marked to place them in
other families, are referred provisionally to the Fucoides." Some other forms appear in the
rock, apparently referable to marine vegetation.
Throughout all the red portions of the rock, no animal remains have been found, with the
exception of fragments of Lingula. Whether the deposition of mud charged with ferruginous
matter was unfavorable to their existence, or whether subsequent causes have obliterated their
remains, it is perhaps not easy to decide. In the Old Red Sandstone, which is equally charged
with the oxide of iron, and often very highly colored, the remains of fishes are perfectly pre-
served; the scales and fins, their teeth and all their solid parts are still in a state of perfect
preservation, and but slightly tinged with the coloring matter. At the present time, we have
no similar deposits in progress extensively enough to determine whether organic forms flourish
under such circumstances. The water flowing from chalybeate springs, and the ferruginous
deposit originating from the same, do not apparently prove obnoxious to the frogs and fishes
that inhabit the pools and streams. -
|
* A species of Fucoid consisting of long slender stems, vertical as to the strata, is found in the town of Penfield, Monroe
county.
48 GEOLOGY OF THE FOURTH DISTRICT.
Erom many circumstances, it would appear that the lower part at least of this deposit was
thrown down rapidly. The quantity and uniform nature of the mass show but one source
for the material for a considerable period of time, there being no alternation or intermixture of
different substances. If we consider the condition of the water rendered turbid by such a
quantity of mud, and highly colored by the iron, it is not surprising if organic forms did not
exist. - - -
In the grey sandstone (second division), animal organic remains are abundant in some places,
though the forms are not numerous. At Medina, in the upper part of this mass, shells of
Lingula, Pleurotomaria and Cytherina occur in great profusion. These likewise occur at
other places, but less abundantly. At that place, in the bed of the stream above the falls, the
Pleurotomaria are crowded together in such numbers as to constitute almost entirely a distinct
stratum several inches thick. The Lingulae and Cytherinae are scarcely less abundant, forming
the greater part of the stratum. In other places these all disappear, except the Lingula, which
preserves its place much longer than the others. Some portions of the rock where these fos-
sils occur is tinged with red, and on decomposing becomes brown, but never of the deep color
of the mass above or below. . -
The following are the more common forms found in this rock, at Medina and Lockport:
1 & 2. Pleurotomaria pervetusta, (a cast.) - 5. Lingula cuneata.
3. Cypricardia alata, 6 & 7. Bellerophon trilobatus, (a cast.)
4. Orbicula parmulata." 8 & 9. Cypricardia orthomota, (a cast.)
Besides the fossils figured, the Cytherina is abundant; there is also a small shell resembling
the Nucula? lavis of Murchison, and an undescribed Avicula, with one or two other shells,
and, rarely, fragments of Orthocerae. Those figured in the woodcut, with the exception of the
Orbicula, are associated at Medina, and we find the same at Lockport. The individuals like
Nos. 3 and 8 are more abundant at Lockport than elsewhere.
In the upper division, the only fossil known is the Dictuolites Beckii of Conrad (Plate I.
fig. 1). This is one of the most interesting fossils found in the rock, often covering large
surfaces with its strong rigid branches and beautiful interlaced rootlets. A remarkable pecu-
liarity of this fossil is the angular or reticulated structure presented by the branches, so unlike
MEDINA SANDSTONE, 49
vegetable forms generally. The spaces produced in this manner are various in form and
unequal in size, as will be seen in the figure, which is a faithful representation of a specimen
from Medina, now in the State Collection. The surfaces of the stratum where this fossil
occurs often present beautifully defined ripple marks. Mr. Conrad thus describes these ap-
pearances: “Upon this surface there is a beautiful fossil, which consists of stems or branches
joined in a reticulated manner, and having undulated lateral root-like fibres. This fossil is
spread over a considerable space, and I noticed that in some instances it followed the undula-
tions of the ripple marks: it was therefore pliable, and moored by its root-like fibres to a
sandy bed, over which a current of water ran, producing such impressions as we see caused
by tidal currents on a sandbar.” - -
Ripple Marks.
These evidences of shallow water do not appear in the lower division of this rock, at any
locality which I have visited; and their absence fully accords with the other facts implying
a rapid deposition in comparatively deep water. Only when we come into the Second divi-
sion of the mass, do we find some imperfect markings of this kind, nor do they occur in any
degree of perfection except in the higher strata, and in few localities. At about the termina-
tion of the quartzose deposit, and in all the higher portions of the rock, they are of frequent
occurrence, and often in great perfection. The specimen from which the accompanying il-
º
| º º º § | § º
ºùi;
º
§§§
| î.
Ripple-marked Sandstone. Medina Falls.
\
- * Geological Report for 1837.
GEOL. 4TH DIST. - 7
50 GEOLOGY OF THE FOURTH DISTRICT.
lustration is taken, was from Medina, a few feet above the position of the Lingula, Cytherina,
&c.; the rock, a variegated quartzose sandstone, showing a slight admixture of the marly
deposit which immediately succeeds. -
In the terminal grey mass at Medina these markings are very beautifully preserved, in con-
nexion with the Dictuolites. Here the longitudinal direction is north-northeast and south-
southwest; and those which the figure represents vary from this but a few degrees, though
the difference was not accurately determined.
These facts indicate a shallow sea during the whole time of the deposition of the upper
part of this rock; and the diagonal lamination is equally a proof of currents in the ocean dur-
ing the same period.
In a few instances, I have met with another kind of surface marking, of which I have
seen no explanation. It is more common in some of the higher groups than in the Medina
sandstone. The illustration No. 8, is from a specimen of this kind.
z
Fº
& E-§
==7
es:ſ g2.ſººº 4.Fº:57. Aº
.#::
AE|:
24::T.&
É
5.5
FºE
#
º
º
-:
*º-
#
|
M
\\
P-, - tº-->
#
j
wº-ºº:
º
ÆE
&#Eº
ºfflººr:
tº sº
sº
Eº
Fe:E. R-
*
The surface of the stone presents undulating ridges, frequently meeting and forming a kind
of irregular network. An appearance somewhat similar is seen where two plane surfaces
with wet clay, or other adhesive substance between, are forcibly separated—the clay is thus
raised in irregular ridges. I have usually referred this appearance to the effect of water eva-
porating from a partially indurated stratum, where the mass below contracts more than the
thin film upon the surface. From the numerous similar facts, together with more pressing
and important details, these have been left without sufficient investigation to form a satisfac-
tory conclusion. On the surface of sandstones, alternating with shales in the Portage and
Chemung groups, this kind of marking is very common, often extending over large spaces.
MEDINA SANDSTONE. 51
*
Sometimes the ridges are much larger than here represented, at others the marking is very
fine, and barely raised above the general level. The same appearance occurs in the Clinton
group, often presenting beautiful specimens, like the tracings of a sculptor's chisel.
Shrinkage Cracks.
These marks, as recent productions, have probably fallen under the observation of every
one, appearing in the clayey beds of shallow pools which have rapidly dried in the sun,
when the mud shrinks and cracks in various directions. Such marks could never be pro-
duced beneath water, and consequently their occurrence in rocky strata affords a clear
inference that the surface in question has been once elevated above the water, and subjected
to atmospheric influence, or perhaps to the sun's rays. As these are usually produced in soft
shaly beds, it requires, for their preservation, that the next deposit be of different material,
and thus casts of the cracks are preserved. Sometimes, however, the cracks themselves are
preserved in the stone. -
Although I have met with no examples of this kind in the neighborhood of Lockport or Me-
dina, where the ripple marks are so well preserved, yet farther east we find them in great
perfection. The mass in which they occur is a soft red shale, and is succeeded by a sandy
deposit. The sand has filled these cracks, and the whole becoming consolidated, the sandy
layer above separates from the shale below, presenting casts of the cracks in strong relief;
as seen in the accompanying illustration.
:=s=#SSESSESssss º E-
§§§s:#ES šºfäº:===
- āşş ÉÉsº
º Sºtsiºsºsºft S$$$:
ÉSºl.
>
ãº:
Eºrº--> gå :
2 -
- - #: 㺠-- :-
a ſºft
#####3:
*::::::::::::::::::: s:S
:-->
És º . Sº
É É%, ſº
Eºs: #s:#S:S §Nāšš %ftº:#####$ e-º
N ############ ÉNNāšā É ºffº ãj
sºsºsºsºsº.º.
Markings of this kind are not of uncommon occurrence in many of the succeeding deposits,
and pa ticularly toward the close of the Onondaga-salt group.
52 ~ GEOLOGY OF THE FOURTH DISTRICT.
Sandy Beach and Stranded Shells.
Among the interesting phenomena attending the deposition of the grey sandstone of the
Second division, are the evidences of a sandy beach which was alternately washed by the
advancing and retiring waves, and again left dry and above their reach. The proofs of this
condition we find in the situation of the shells of Lingula, spread upon the surface, and the wave-
lines, which mark the successive layers. -
In the open quarries at Lockport where extensive surfaces of the smooth layers are exposed,
an observer will notice the shells of Lingula cuneata, curiously distributed, each with a little
ridge of stony matter extending from the beak, narrowing and sloping down to the general
level of the stone. .
The analogy of this little sloping ridge of stone to what we see formed in shallow currents,
or where waves are washing a beach, and meet some obstruction, as a pebble, is too obvious
to be mistaken; and the observer at once feels that he has discovered unerring marks of the
course of the current, at the period when this rock was deposited. The beaks of the Lingula
are all directed to the N.N.W. or varying from this to N. by W. half W. This perfect pa-
rallelism, where hundreds may be seen on the surface of a single slab, is very striking. -
At first these shells appear as if they might have been living, and anchored to the sandy
bottom by their peduncles; but further examination has proved that they are all single valves,
and must have been floated into their present situation, and strewed, by the waves or the current,
evenly over the sandy surface. They all present the outer or convex side of the shell up-
wards, and this is the position they would naturally take under the circumstances. After
being thus left, and adhering firmly to the sand, the current or advancing tide swept over them
again without the power of removing them from their position. The consequence would then
be the production of a little ridge of sand, extending from the beak of the shell in the direc-
tion of the current. -
10.
ºffl
t|
|
|
MEDINA SANDSTONE, - 53
The figure No. 10 is a representation of a small specimen with three shells of the Lingula
cuneata, each with the little ridge of stony matter as described, extending from its beak. It
will be recollected, also, that it is not to the surface of a single layer or stratum that these
shells are confined. They appear upon successive strata for many feet in thickness, and they
are sometimes separated from each other by a deposit of less than half an inch. These cir-
cumstances prove the operation of similar causes during a long period of time. Each suc-
ceeding layer retains the impressions in a very beautiful manner, and thus we often obtain
specimens with shells upon the upper side, and casts upon the side below. Several large
slabs of this kind may be seen in the State collection. ~. -
The evidence from these drifted shells, with their ridges of stony matter, corroborates the
inference drawn from the condition of the fossils at Medina. It will be noticed, also, that the
position of the fossils at the latter place is east a little south from the quarries near Lockport,
of which we have been speaking. The direction of the current as there indicated would have
a tendency to drift all the shells in a south and easterly direction. Since this mass has once
extended much farther north than at present, as is evident from its abrupt outcrop, and the
great excavation of the lake valley, it is quite probable that Medina was brought within the
range of the current from the N.N.W., and that from the proximity of land or very shallow
water, the fossils accumulated as there described. - -
The Lingulae are not alone in the production of these appearances upon the surface; in
some instances we find small fragments or pebbles of a greenish shaly sandstone, precisely
like some parts of the lower mass, which seem to have been stranded in like manner as the
shells. This is seen in the specimen of which Plate II. is a representation. In this instance
three of the largest obstacles are fragments of green shaly sandstone, and the others shells
of the Lingula. -
It might appear from what is here stated, that there is a discrepancy in the direction of the
water as indicated by the Lingulae, the little ridge of sand pointing northwardly, while the
fossils are accumulated in a southeasterly direction. The explanation seems to me to be this,
though some other view may be adopted: The surface on which the shells were Stranded, was
a long low beach or sandbar washed by the waves of the ocean, as will be seen by further
illustration. The shells were carried forward by the waves, which advanced high up the
beach; with the retiring wave, all these would be moved backward a short distance, but would
soon be left attached to the sand, the water of the still retiring wave scooping out the depres-
sion in front and at the side, and piling up the little ridge beyond the beak. In this manner,
the direction apparently indicated is opposite the real direction of the force which transported
the specimens. That such is the process by which shells and pebbles are stranded on the
present beaches, any one will be convinced by observation. By the retiring of the wave, also,
any single valve of a bivalve shell, which may remain with the outer side downwards, will
surely be overturned, and at last usually remain in the reverse position, as is the case with
all the shells of the Lingula on the sandstone. After being once fixed in this manner, they
are not easily removed by succeeding waves. - - -
The surfaces of these slabs upon which the shells are found have often a beautiful clouded
MEDINA SANDSTONE, - 55
The woodcut No. 11 is an illustration of these lines as they appear upon a slab about
five feet in length. The course varies but little in the numerous instances which I have
examined. A line perpendicular to the curve generally gives a direction differing but little
from N.N.W. and S.S.E.; which shows that the direction of the wind varied between north-
west and north, and that the line of beach must have been nearly at right angles with this
direction, which corresponds very generally with the present line of outcrop of this rock.
Existing phenomena of the character here described may be witnessed every day upon the
shores of the ocean, or of the larger lakes. Any one who has passed along a sandy beach
during the ebbing of the tide, or when toward evening the fresh breeze of the day is lulling,
must have observed as the waves roll in and extend far up in a thin sheet of water, that the
crest of each one forces on before it a film of sand. This, when it has arrived at its extreme
limit, and during the moment which elapses between its advancing and retreating motion, is
deposited in the form of a minute ridge or line, defining perfectly the outline of the wave.
These occur one after the other, sometimes crossing and sometimes parallel, but always
marking the limit of the water. Often after many of these are formed, a wave advancing
beyond the others, obliterates the whole, and leaves its own line far above them; and if its out-
line do not correspond with the previous ones, those portions of the formerlines are left limited
by the last. When the beach dries rapidly from the heat of the sun, these are distinctly seen,
preserving most perfectly the outline of the wave in all its minute curvings and undulations.
So minute are the ridges, and the amount of matter so small, that a gentle wind is sufficient
to remove the whole, and it might seem almost fanciful to suppose that any vestiges of them
are preserved; yet after having made repeated observations upon these wave lines, and upon
the markings on the strata in the quarries at Lockport, I was forced to the conclusion that the
cause of both was identical. During the past summer I examined these quarries, and also
the recent operation upon the sandy beaches of Lakes Ontario and Erie, in company with
Mr. Lyell, and I now have the pleasure of recording his opinion as coinciding with what has
been expressed; namely, that the cause producing the markings upon the sandstone is iden-
tical with that producing wave lines upon our present beaches.
In several places west of the Genesee river, on the shore of Lake Ontario, are large bays
or ponds, separated from the lake only by a sandy beach, and usually having a narrow outlet,
or sometimes none at all, for a considerable time, until the accumulation of water inside forces
a passage through the sand. At one of these places, there was a broad flat beach, rising
but little above the level of the lake, and sloping gently back to the marshy margin of the
pond. A previous high wind had raised the lake, and the heavy waves had washed entirely
across this beach into the pond. The surface beyond the highest point where the water flowed
smoothly down, was covered with pebbles, some fragments of shells, and the bones and scales
of fishes. Every one of these had offered some obstruction to the advancing water; and in
that direction, and on each side, there was a depression or shallow excavation, while beyond
the obstacle extended a little ridge of sand narrowing and sloping down to the general surface.
56 - GEOLOGY OF THE FOURTH DISTRICT.
The illustration in the margin exhibits the most pºſed analogy to
the appearances before described.
On the side toward the lake the surface of the sand was marked
with wave-lines, as well as the ridges, exhibiting all the phenomena
described, and showing the most perfect analogy with the same
appearances upon the strata of the Medina sandstone at Lockport.
The illustration No. 13 is from this place, and hundreds of similar ones might have been
copied from the sand in the space of a few rods. A heron (Ardea Herodias) had been walking
upon the spot but a short time before, and one of the footsteps is represented as it actually
appeared in connexion with the wave-lines. In this instance parts of three distinct series of
curves are represented." ar
w
aw)
A
|
Wave-lines on Sand-beach. Long pon
M.
, Monroe connty.
Should any one doubt the possibility of such slight markings being preserved, he has only
to examine the beautiful series of curved lines upon the surface of the strata in the quarries,
and thence transport himself to a smooth sandy beach upon the lake shore, and the phenomena
exhibited will not fail to convince him that the cause there operating, has also been one of the
active powers of nature, in those periods during which few records have been preserved of
the relative situation and distribution of sea and shore.
Without desiring to dwell too long on a subject that has been to me of the most thrilling
interest, I have still the desire to give all the illustration and elucidation it requires, and to
direct the attention of observers to similar appearances in the older strata, by which, per-
haps, we may be able to explain more satisfactorily many circumstances attending their for-
mation. - - - t -
All the appearances enumerated seem corroborative one of another; the Lingulae, which are
a deep water shell, have been drifted, the valves separated and strewn upon the sand; the
clouded and mottled surface, and lastly the wave-lines, indicate very clearly that the deposit
* It may sometimes be observed that a wave advancing obliquely upon a beach removes the sand as far as it reaches, leaving a
depression seaward; this happens if the sand be light, or saturated with water, and may perhaps take place under other circum-
stances, but it is only an exception to the general rule.
MEDINA SANDSTONE, 57
has been successively a beach washed by waves, and again covered with deposits of sand by
the returning waters.
In standing upon the exposed surface of the quarry, one can almost fancy himself still
upon the shore of some quiet bay or arm of the sea, where the waves of the receding tide
have left these little ridges of sand, which on their return will be obliterated and mingled
with the mass around. The shells and fragments, and the clouded sand, all lie around him
with a freshness of appearance that might almost make him doubt. But his foot is upon the
firm rock, and his hand cannot obliterate the faint waveline, nor remove a single shell from its
place. Every thing is firm and fixed, and he is forced to recollect that millions of ages have
rolled on, since the sea washed this shore, and the shells lay upon the glistening sand as he
may have seen them in the haunts of his childhood. How beautiful, how simple, and how
grand is this exhibition; and how much does it illumine the mind as to the mode of produc-
tion of these older formations which have been considered so obscure. Here was an ocean
supplied with all the materials for forming rocky strata: in its deeper parts were going on
the finer depositions, and on its shores were produced the sandy beaches, and the pebbly
banks. All, for aught we know, was as bright and beautiful as upon our ocean shores of the
present day; the tide ebbed and flowed, its waters ruffled by the gentle breeze, and nature
wrought in all her various forms as at the present time, though man was not there to say,
how beautiful
GEOL. 4TH DIST. - 8
58 GEOLOGY OF THE FOURTH DISTRICT,
10. CLINTON GROUP.
Lower part of the Protean group of the Annual Reports; Ferriferous slate, and Ferriferous
- sandrock of EATON.
(Part of No. 5, PENNsyLVANIA SURVEY.)
This group is one of variable character, consisting of many kinds of deposits, which are
not uniform either as to composition or continuation. From this circumstance it first received
the name of Protean. This term, also, at that time included the Niagara group, which
appears a thin mass in the Third district; but from its greater development and distinctive
features in the western portion of the State, that has been separated.
The term Protean is still applicable to this assemblage, which in some places consists of
thin shaly sandstones, shales, and even conglomerates; in others, of thin-bedded, impure lime-
stones, shaly sandstones, iron ores, etc., with scarcely any fossils except Fucoides; still
again it appears as a duplicate series of shales, limestones and iron ores, with some inter-
mixture of sandy matter, all containing abundance of marine shells; and lastly, it presents
itself on the extreme western margin of the State, as a single bed of shale and limestone,
with rarely a fossil of any kind. From its superior development near the village of Clinton,
in the Third district, it has received that name.
It will be seen that this formation, which is colored green upon the map, extends across
the district in a nearly east and west direction, occupying a narrow belt of country just above
and to the south of the Medina sandstone. Its greatest width within the district is in Wayne
county, and it thins gradually towards the west. Through the greater part of Wayne county,
this formation ranges within two miles of the lake shore. Crossing the Genesee below
Rochester, it forms for a few miles a low terrace on the north side of the canal, known along
that distance as “the Little Ridge.” After that it is seen on the south side to within eight
miles of Lockport, where the canal is excavated in the rocks of the group; thence westward
it appears near the base of the limestone terrace, forming part of the slope. Beyond the
Niagara river, in Canada, it can be traced, still of the same character as within the State ; and
it probably follows the associated rocks through the peninsula.
This formation exists in Ohio, though not so distinctly developed as in New-York. Dr.
Locke has detected some of the peculiar fossils, as well as the iron ore, in Clinton county of
that State; and from numerous other facts, it appears to have a wide range and very variable
lithological character. In Pennsylvania the whole formation is greatly thicker than in New-
York; but the products bear a close resemblance. It is there known as the “red and varie-
gated shales and sandstones.” e
From the destructible nature of its lower member in the Fourth district, it has usually
receded some distance from the outcropping edge of the sandstone, and it is only along the
CLINTON GROUP. 59
water-courses that we find it disclosed. The whole group has for the most part been so
denuded as to form no prominent line, but enters into the general equal descent of the country
toward the lake. º i
The harder members of the group appear in all the ravines and water-courses, forming
rapids, or low falls. These also sometimes appear in the more level country, and are exca-
wated for wall stones.
The greater part of the group is well developed on a small stream near the former Shaker
settlement at Sodus bay, and more perfectly, just above the lower falls of the Genesee. At
this place the mass admits of the following subdivisions, in the ascending order:
1. Green shale resting on the Grey band, destitute of fossils, very fissile and unctuous.
2. Oolitic iron ore with concretions, fragments of shells, corals, etc. A few thin layers of impure
limestone or shaly sandstone, sometimes intervene between the shale and iron ore.
3. Pentamerus limestone, a siliceous or calcareous amss with thin Sandy layers, often having the charac-
ter of shaly sandstone. It also contains bands of hornstone or chert, consisting mostly of silici-
fied fragments of fossils. This part of the mass is distinctly marked by the presence of large
numbers of the Pentamerus oblongus, sometimes crowded together, forming a band a foot or
more in thickness, or distributed through the whole rock.
4. A green shale similar to that below, though of a less deep color. It also exhibits one or two bands
of limestone, composed mostly of shells of Atrypa hemispherica, which preserves its beautiful
pearly lustre. It contains Graptolites, and in some localities where these abound the mass is
black,
In this relative situation in Wayne county, the second bed of iron ore occurs. The ore is
more perfectly oolitic than that below, and with fewer concretions, and usually less carbonate of
lime intermixed. It appears at Wolcott furnace, and is apparently the bed wrought six miles
farther east.
5. A limestone similar to the more calcareous portions of No. 3; and at Rochester containing few fossils
except crinoidal joints; it is usually thin-bedded, the layers separated by shale; it contains numerous
cavities filled or partially filled with sulphate of lime, sulphate of baryta, iron pyrites, etc.
From its situation as the separating mass, it partakes also of the character of the next succeeding
group. The Niagara, however, being so well characterized, and the Clinton group an ac-
knowledged variable one, it is thought better to place it with the latter.
The same essential order in the parts of the group appertains to it in several localities in
Wayne county, but west of the Genesee river two or more of its members are wanting. The
shale and calcareous matter seem equally persistent, but both gradually diminish westward.
1. LowLR GREEN SHALE.
This mass is known by its bright green color, and its strong contrast to the subjacent rock.
It is found in the eastern part of Wayne county, not exceeding thirty feet thick. It is marked
towards its centre by a band of purple shale at Sodus point, and numerous localities in the
60 GEOLOGY OF THE FOURTH DISTRICT,
|
same neighborhood. In some places in the western part of Wayne county, it diminishes and
nearly disappears, and again continues of variable thickness. On the Genesee river it is twenty-
three feet thick; farther west, at Medina, it is about three feet; while at Lockport it is
scarcely visible, or intermixed with the terminal mass of the Medina sandstone. Again, on
the Niagara river it has a thickness of four feet. Wherever seen it exhibits its predominating
character, as a soft green argillaceous shale, splitting into thin laminae, and crumbling rapidly
on exposure.
At Sodus, and other places in Wayne county, where this rock is well exposed, it contains
thin wedge-form layers of limestone of small extent, which are fossiliferous as well as the
shale itself, containing large numbers of crinoidal joints, and fragments of drifted shells and
corals, as well as perfect specimens. These are sometimes replaced by carbonate of iron,
and the substitution is so entire that the crystalline structure is as perfectly preserved as in
those of carbonate of lime. l
On the Genesee river, the mass is a pure argillace0us shale, entirely free from any calca-
reous intermixture, and contains no fossils. At this place, it forms a distinct green band in
the river bank at the lower falls; and between this and the middle falls is seen both in the
bed and banks of the stream. Below the falls, it forms the same distinct band for a mile or
two farther north, and is well exhibited in the road leading from the brow of the hill to the
steamboat landing. On exposure it crumbles rapidly into thin minute fragments, and in wet
weather forms a tenacious greenish mud.
2. OOLITIC OR LENTICULAR IRoN ORE.
Argillaceous iron ore of EATON, including the lenticular and jaspery varieties. Lenticular clay iron
ore of Dr. BECK, Fossiliferous iron ore of the Pennsylvania Survey.
Succeeding the green shale upon the Genesee river, is a thin bed of iron ore; this is not
present in all situations, its place being sometimes marked by the slightly ferruginous color
of the upper part of the shale, or lower part of the limestone above. The quantity of the
material seems to have been very small, and from its nature widely diffused; it probably
existed in the menstruum, which at the same time held in suspension the materials forming
the other associated deposits. In some instances, it has forced its way through all the upper
deposits and rests on the lower shale, and in other cases the upper shale has arrested its pro-
gress. It appears to have been intermingled with both the limestones, and probably separated
from them by its greater specific gravity, falling to the bottom, where the shaly matter had
become too firm for its farther descent.
The purple or brownish band which marks the lower green shale at Sodus point, while the
iron ore is there absent, and again, the fossils of that division replaced by carbonate of iron,
sufficiently prove the intimate mixture and diffusion of the ferruginous matter through the
whole.
In the town of Ontario, Wayne county, this bed of ore attains its greatest thickness, which
CLINTON GROUP. 61.
is about two feet. Between this place and the Genesee river, it is scarcely to be found ex-
posed, though constantly near the surface. On the Genesee, its thickness is about fourteen
inches, showing a diminution from Ontario of ten inches in about twenty miles. Westward
from the Genesee, the rock immediately above is often ferruginous, but I have nowhere seen
the ore as a separate stratum. At Medina, Albion, Lockport and other places which offer
good sections, as far west as the Niagara river, the ore is absent. s
This diminution and final disappearance westward would indicate the place of its origin to
be farther east, and beyond the limits of the Fourth district. The existence of large beds of
specular and micaceous ore on the northwestern slope of the primary chain of northern
New-York, where denudation has been extensive, and large quantities removed, may be the
source. A more probable origin of the ore, however, is in the decomposition of iron pyrites,
and the production of this oxide of iron. The oolitic form seems, according to the facts pre-
sented by Mr. Wanuxem, due to the influence of thermal waters. Such a condition of the
menstruum would hasten the decomposition of the pyrites and the formation of the oolitic ore.
The second bed of iron ore appears but in few places in the Fourth district, and in all
except one locality is too thin to be of economical importance. Another fact which is some-
what remarkable, is that the two beds never appear in succession at the same locality, or in
the same line of section. In places where the lower one occurs, the upper is wanting; and
where the upper occurs, the lower one is not found. This circumstance farther confirms the
opinion, that the materials were in a state of mechanical suspension, and the place of their
final deposition only determined by the solidification of the strata which opposed their descent.
The deposition of all matter forming rocky strata would take place inversely as their solu-
bility, if in solution, and directly as their specific gravity, if in suspension. The ore is rarely
if ever found diffused through the shale, except where that mass contains calcareous matter;
but in such points it often pervades several feet in thickness. The iron and carbonate of lime,
from their nature, would remain much longer in the menstruum than the clay. The iron,
though more soluble than the calcareous matter, would still be carried down by that body on
its deposition, and thus what forms a thin band of ore in one place may be diffused through
several feet of calcareous strata in another.
The Wolcott ore bed, which is wrought to supply the furnace in that town, appears, so far
as I can examine the rocks above and below it, to be the upper of the beds mentioned. Its
thickness is much greater here than elsewhere, and it is succeeded by a shaly rock containing
a peculiar association of fossils.
At Wolcott furnace, six miles west of this, the upper ore bed is but a few inches thick, and
quite insufficient for working; it is seen in the creek, associated with thin beds of impure
limestone, shale, etc. At this place it is impossible to ascertain whether the lower bed occurs
or not, but in excavations in the Pentamerus limestone there has been no iron ore seen, or at
least none has been thrown out with the limestone. In several other localities between this
place and Sodus point, iron ore has been discovered, but so far as I could ascertain they are
62 GEOLOGY OF THE FOURTH DISTRICT.
all of the upper bed." At the Shaker village, Sodus point, the position of the upper bed was
not distinctly visible, though all the deposits below were so. Upon excavating the earth,
large masses of ore were obtained; and though from the quantity of fragments of the superior
rock, I did not find the ore actually in place, there is still scarcely a doubt of its existence at
that spot. Its place is in the bed and banks of the stream a few rods above the mill-dam.
The place of the lower bed is here distinctly seen, but the ore is absent, its only represen-
tative being the small quantity of carbonate of iron disseminated in the limestone above.
I have not been able to discover the upper bed west of this place; the next locality exhibits
a thinning of the lower green shale, with the ore intermixed with the Pentamerus limestone.
North of Sodus village, and in the town of Ontario, the ore is evidently from the lower bed,
the Pentamerus limestone always appearing above. The last place westward where the ore
is seen as already mentioned, is the lower bed, on the Genesee.
3. PENTAMERUs LIMESTONE OF CLINTON GROUP.f
This mass, in some places, is composed almost entirely of thin beds of impure limestone,
which alternate with thin layers or laminae of green shale; in other places it is a nearly pure
crystalline limestone, composed of broken valves of Pentamera and other shells, with a large
proportion of crinoidal joints. The latter character prevails in some places in the eastern part
of Wayne county, and is seen distinctly at Whiting's mill, three miles west of Wolcott fur-
nace. To this structure, producing unequal expansion of the crystalline and uncrystalline por-
tions, is due its power of withstanding heat, which has brought it into use as an ordinary fire-
stone for chimneys, hearths, and some of the less exposed parts of furnaces.
At Sodus point, and a mile northeast of Wolcott furnace, the shells of Pentamerus are
imbedded in a shaly mass, with just sufficient calcareous matter to make it firmly cohere.
North of Sodus village the mass is free from argillaceous matter.
On the Genesee river this rock outcrops in the banks on either side, and stretches across
the stream, forming the middle falls. In this situation we find less shale, but an intermixture
of shaly and calcareous sandstone, which in some places predominates. Much of the mass
is a crystalline siliceous limestone, very compact and tough, forming excellent building mate-
rials, but difficult, from its hardness, to work. The predominating siliceous character at this
locality, induced Prof. Eaton to give it the name of Ferriferous sandrock; this term cannot
be retained, from the fact that in nearly all localities examined it is comparatively free from
sand, and its distinctive feature is calcareous.
In numerous localities in Monroe county it appears as a limestone, and is quarried in many
places for the same uses as in Wayne county. The Pentamerus, on the Genesee, is confined
* In some places, from the proximity of the Lake level, it is impossible to ascertain without boring, whether the lower stratum
of ore does exist or not.
# This term is used in this manner to avoid confusion, the term Pentamerus limestone being used to designate that mass
charged with Pentamerus galeatus in the Helderberg series.
g
§ 4.23 - 1.
§tº
§
CLINTON GROUP. 63
to a small portion of the rock, and seems gradually to disappear farther westward. In Orleans
county the same limestone is entirely destitute of this fossil, but is readily recognized by posi-
tion and other characters. In many places in Wayne and Monroe counties it contains nodules
of hornstone, which sometimes assume the form of calcedony. This matter increases so
much in Orleans and Niagara counties, that it forms thin layers alternating with the lime-
stone. Associated with this chert are commonly found silicified fragments of shells and cri-
noidal joints. At Rochester, distinct layers are entirely composed of the silicified shells of a
species of Strophomena.
One mile south of Medina, in the bed of the stream, the limestone is seen separated from
the upper member of the Medina sandstone by only three feet of shale. At that locality, the
rock is composed of thin irregular layers of impure limestone with much hornstone; the
courses are separated by shale, which in the exposed banks of the stream has dissolved out,
and left the solid parts piled loosely together like a stone wall. The Pentamerus is not here
found, but the rock is abundantly charged with other fossils, particularly the Atrypa congesta,
which is rare on the Genesee. About eight miles east of Lockport it is excavated from the
bed of the canal for some distance, where it is composed of thin irregular layers of impure
limestone and greenish shale, with much hornstone. When we arrive at Lockport, it becomes
evident, that from the thinning of the Second green shale of the Rochester section, the two
limestones have come together ; the Pentamerus division forming but a few feet of the cherty
layers in the lower part of the mass. This might have been expected from the thinning of
the lower shale at Medina; and at that place there is no evidence of the existence of the upper
shale, though the absolute contact of the two limestones cannot be determined. From Lock-
port, the Pentamerus portion continues to form the lower layers of what is thence one mass
of limestone; and it appears in like manner and situation on the Niagara river. At Lockport
it has become nearly destitute of fossils, and on the Niagara river it is entirely so, with the
exception of crinoidal joints. The lower part of the limestone, as it appears on the Niagara
river, is highly magnesian, and from the presence of iron pyrites rapidly decomposes, giving
rise to the production of sulphate of magnesia, which at favorable points, along the overhanging
mass upon the river bank, may be collected in quantities of several pounds.
What changes this rock may assume beyond the district is uncertain; so far as traced in
Canada, it maintains the same characters as on the Niagara river. We know, however, that
in the southwest part of Ohio, and in Indiana near the junction of the Blue and Cliff forma-
tions (of the Ohio reports), there is a limestone charged with Pentamerus oblongus. The
same continues westward, and is seen in Wisconsin and Iowa. From this it is evident, that
while this fossil and the mass to which it is confined nearly disappear within New-York, there
is a reappearance of the same at the southwest and west; and that whatever may have been
the cause of its non-existence in the western counties and in Canada, it still was living in a
remote part of the ocean in great profusion, and perhaps undisturbed by the causes which put
an end to its existence here. It was before remarked that the shells of this fossil are nearly all
broken, and the valves packed together as if drifted or washed by the waves, few perfect ones
being found. At the west, on the contrary, the larger number appear to be perfect; and
|
64 GEOLOGY OF THE FOURTH DISTRICT.
though in some localities they may have been drifted, still, as a general rule, they have not
suffered violent removal. This furnishes, among others, an example of a formation which,
after thinning partially or entirely, reáppears in the same direction, even better exhibited than
in the first locality. Although the group is much more developed in the Third district, still
the Pentamerus appears but rarely, and attains its greatest perfection in Wayne county.
4. SECOND GREEN SHALE.
This is readily distinguished from the lower green shale by its less deep color, and from
being everywhere fossiliferous, while the lower is so only in a few localities. The change is
very abrupt from the limestone below to this soft green shale. At Rochester, this mass has
a thickness of twenty-four feet, and it maintains nearly the same in other places. At Wol-
cott, however, it appears to be somewhat thicker, though its upper limit was not distinctly
ascertained. It is well exposed at Wolcott furnace in the banks of the creek; it also appears at
the ore bed six miles farther east. At Sodus point it is well exhibited, and large specimens
may be obtained covered with Graptolites. Its whole thickness is seen in the Genesee river
below the upper falls at Rochester. From this point it diminishes westward, and entirely
disappears, as before mentioned, leaving the two limestones in contact.
At Rochester and other places, the mass embraces a band of purple shale three or four
feet thick, differing from that around it only in color. A few feet higher it is marked by a
line of black, containing Graptolites. This portion is usually exceedingly brittle, apparently
from the presence of carbonaceous matter. -
About six feet from the top of the green shale, are two, or in some places three, thin bands
of calcareous matter, three or four inches thick, composed entirely of shells, principally the
Atrypa hemispherica, which still preserves its original lustre, giving the whole mass a pearly or
silvery hue. Very beautiful specimens are obtained from these bands, presenting an entire
surface of the shells; it is rarely, however, that perfect shells are found. They seem to have
been drifted together in great numbers, and the valves are often separated. Like the Penta-
merus below, they indicate a period when the tranquillity of the waters was disturbed, or
when from some other cause this portion had become the margin of the sea.
Throughout the deposition of this shale, however, the ocean appears to have been quiet:
the mass consists of finely levigated mud, which would not have been deposited during a pe-
riod of much disturbance. The condition of the fossils usually indicates a very quiet state of
the waters; when imbedded in the shale, every part is found in great perfection. The deli-
cate structure of the Graptolites, which apparently the least agitation would destroy, is gene-
rally preserved very entire. - -
The upper part of this mass is often deeply stained externally by oxide of iron, though the
bed is entirely wanting. The stain of iron prevails more or less throughout, penetrating all
the slaty divisions, and often forming a thin enamel over the green surface. I have seen no
minerals in this rock, except in the thin calcareous bands, where sulphuret of iron, sulphate of
CLINTON GROUP. 65
baryta, and crystals of carbonate of lime sometimes occur, the two latter in small nests or
cavities.
5. UPPER LIMESTONE OF CLINTON GROUP.
The second green shale, like the first, is terminated above by an impure, thin-bedded cal-
careous deposit; the layers, which are often exceedingly tough, are separated by narrow
seams of green shale. This rock closely resembles the more calcareous portions of the lower
limestone. In some localities it contains masses and nodules of iron pyrites, which, on de-
composing, leave the spaces filled with anhydrous gypsum, and these sometimes occur in
such profusion as to render the rock useless for building purposes. Again, it is more sparingly
diffused, and only sufficient to discolor the surface on weathering. The lower part of this
limestone is often deeply stained with iron from the decomposition of pyrites; and from the
general similarity of the two calcareous masses, one is often led to suspect the occurrence of
a bed of iron ore in a similar situation. Toward the Niagara river it becomes more entirely
calcareous, and contains less sulphuret of iron.
Some of the strata are of crystalline structure, and greyish blue color, composed in a great
degree of comminuted corals or other organic remains. From its unequal crystallization it
becomes, like the Pentamerus mass below, a good fire-stone. This character, however, with
the intermixture of siliceous and argillaceous earths, makes it generally unfit to be burned for
lime. ^ - -
This division is eighteen feet four inches thick on the Genesee river, and continues through-
out the district more uniformly than either of the others; showing about twenty feet on the
|Niagara. In many places it extends beyond the base of the great Limestone terrace, and
forms a narrow plateau to the west of Rochester, often quite exposed from the removal of the
superincumbent earth.
The more uncrystalline portions of this limestone dissolve on weathering, and leave the
crystallized joints of crinoidea, corals and other fossils, standing out in bold relief. Thus is
revealed in a clear manner the materials of the rock, as well as the changes that have been
wrought upon them. These fragments of shells, crinoids and corals must once have formed
parts of living and perfect individuals, which have lived at the bottom of the ocean, beyond
the reach of the destructive agency of the waves; again they have been brought within such
influence, and broken down, and their fragments ground together, till they formed the homo-
geneous mass presented to the eye in the great body of this rock. Afterwards these materials
must have constituted a beach, or bar of calcareous sand, extending beyond the limits of
the district in either direction. This is the process of formation not only of this individual
mass, but of nearly all calcareous deposits. The close alternation of deposits of purely argil-
laceous matter, with those of calcareous composition, is another subject of the highest interest
to the student in these subjects; they indicate changes in the depth of the ocean which have
marked the different periods; and they direct us to the influence of causes which are now in
operation upon the solid crust of the earth, and visible only by their effects in elevating or
depressing the bed of the ocean.
GEOL. 4TH DIST. 9
66 GEOLOGY OF THE FOURTH DISTRICT.
Localities. – The most easterly exposure of the rocks of this group within the district, is
at the Wolcott ore bed, where some of the higher shale with fossils, as well as the iron ore,
is found. Near Red-Creek village we find the green shale with fossils; at Wolcott furnace,
the Pentamerus mass and the green shale above; and at Whiting's mill, three miles west of
this place, the Pentamerus mass and lower green shale are seen. At Sodus point we find the
iron ore and associated shales and limestone. At the former Shaker settlement on Little
Sodus bay, all the members of the group, except the iron ores, are well exhibited, and this is
one of the best localities in Wayne county for its examination. The Pentamerus mass forms
a fall of twelve feet in the stream at that place; the green shale, with fossils, appears below,
in the bed and banks of the creek; and above the fall, the higher green shale with Grapto-
lites, and the upper limestone with Atrypa, are both seen.
In the eastern part of Williamson, a little north of the Ridge road, the green shale with
Graptolites occurs, and a short distance to the north of this, the Pentamerus limestone.
North of Sodus village the Pentamerus limestone and iron ore appear in several places.
On Salmon creek, above the forge, the iron ore, green shale and Pentamerus limestone are
all exposed, and still farther up the stream are found the thin calcareous layers with Atrypa
hemispherica. Again at Ontario, just north of the Ridge road, the green shale with fossils
may be seen; and finally, almost every stream north of the road from Wolcott to Rochester,
exposes one or more members of the group. -
In Monroe county, the group appears near the head of Irondequoit bay, and again in the
banks of the Genesee, which is its best exposure in the district. The canal is excavated in
the same for some distance, about twelve miles from Rochester. In Sweden it is éxposed on
a small stream which crosses the canal a little west of Adams' basin. There are also a few
other localities, but the exposure is meagre. -
In Orleans county, some of its members are seen in the stream south of Albion; also on
the Oak-orchard creek, a mile south of Medina, the mass is well exposed, this being the best
locality for order of superposition west of Rochester. tº
In Niagara county, the limestone appears near the village of Middleport, where a small
stream crosses it. A short distance west of Reynolds' basin, the canal was excavated in the
group, and the piles of fragments of the impure limestones, shaly matter, and hornstone,
with numerous fossils, render this an attractive spot. Passing on to Lockport, we find the
same rock exposed in the banks of the stream below the village, and, as before remarked,
nearly the whole group is represented by the limestone. The limestone and the thin mass of
lower green shale are seen in the escarpment at numerous points between Lockport and Lew-
iston, where it crops out in the river bank.
Thickness. – The thickness of the whole group in Wayne county, wherever it can be
measured, is somewhat less than eighty feet; and in some places, from the thinning of the
shale, it is little more than sixty feet. On the Genesee river, its different members appear as
follows:
CLINTON GROUP, 67
Feet. Inches.
5. Upper limestone, . . . . . . . . . . . . . . . . . . . . . . . . . . . . 18 4
4. Upper green shale, . . . . . . . . . . . . . . . . . . . . . . . . . . . . 24.00
3. Pentamerus limestone, . . . . . . . . . . . ............ 14 00
2. Iron ore bed,. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 0 14
1. Lower green shale, . . . . . . . . . . . . . . . . . . . . . . . . . . 23 00
80 6
At Lockport the calcareous portion is about twenty feet thick, and the shale scarcely defi-
nable, apparently mingled with the terminal part of the Medina sandstone. On the Niagara
river the limestone is twenty-five feet thick, and the shale below four feet. -
Mineral Contents of the Group.
The first mineral which meets the eye is the hornstone of the Pentamerus mass; this often
passes into translucent varieties, and forms little cavities lined with calcedony. Fossils which
are enclosed in the mass, frequently, on breaking, present a cavity lined with delicate quartz
crystals, or calcedony. At Rochester large geodes have been found lined with this mineral,
in mammillary or botryoidal forms, producing beautiful specimens. Siliceous sinter and
cacholong both occur in the same association, and Prof. Dewey mentions carnelian as occur-
ring here. * -
The sulphates of baryta, and of lime, are both found in the rocks of this group, and in several
localities. The sulphate of baryta occurs in spheroidal cavities in the Pentamerus mass, and
more rarely in the upper limestone. Groups of crystals, and cavities lined with the same, of
a beautiful flesh-red color, occur in the oolitic iron ore at Wolcott, and more rarely with
the ore in other places. Crystallized carbonate of lime is found with the sulphate of baryta,
and in other situations. The sulphate of lime is principally confined to the upper limestone,
where it often forms masses of considerable size, partially filling cavities which have appa-
rently resulted from the decomposition of iron pyrites. Pyritous copper and green carbonate
of copper occur in the Pentamerus mass, and Prof. Dewey has discovered some spiculae of
native copper in the same rock. I have detected the green carbonate of copper in cavities in
the calcedony or sinter, at Medina and near Reynolds' basin.
Mud Casts. – The lower strata of the Pentamerus mass, on the Genesee, are of a shaly
sandstone; these, when in contact with the shale below, often present surfaces curiously con-
torted and twisted. They appear as if they had been in a semi-fluid state, and forced along
over the yielding mud, previously rendered uneven by the flowing of water over the surface, by
which little depressions had been scooped out at short intervals, and into these the subsequent
mass was deposited. -
Another appearance attending these lower strata, is the occurrence upon their under side
of long straight, or slightly tortuous ridges, standing out in bold relief upon the slab. These
I have denominated casts of mud-furrows, and suppose them to have been made in depressions
68 º GEOLOGY OF THE FOURTH DISTRICT.
previously existing in the mud, and filled by the subsequently deposited matter. These are
of more common occurrence in the rocks of the Portage group, where they will receive illus-
tration. Whatever may have been their origin at the period of the Clinton group, they appear
to be widely extended. When in Ohio, Dr. Locke showed me specimens of precisely similar
character, and from the same position in that State. They were likewise associated with thin
layers, containing numerous crinoidal joints, identical with those so abundant in the same rock
at Medina, Lockport and elsewhere. The influences operating upon the bottom of the ocean
at these two distant points, are thus proved to have been the same.
Organic Remains of the Clinton Group.
This group is for the most part well marked by its fossil contents, and presents an inte-
resting series of organic remains. From the varying character of its lithological productions,
however, the fossils are not so constant in their occurrence as in other rocks; and if the group
be examined at distant intervals, scarcely a fossil will be recognized as common to the two
localities. A portion of the mass at one place well marked by certain species, may be desti-
tute of fossils at another, or present, for the most part, a different assemblage. It becomes
very evident, therefore, that lithological development has had much to do with the occurrence
and nature of the fossils, as well as their abundance. It has already been seen that the
products of the group fail in a western direction, and at the same time the character of the
fossils changes in an equal degree. On the Niagara river, the only fossil which can be said
to continue from the eastern extremity of the district, is the peculiar Crinoid of which we
find the numerous joints; and these indeed may have been drifted to their present situation.
This crinoidal joint (fig. 5, woodcut No. 16), is abundant in nearly all situations, and though
apparently an insignificant object, the observer will find it of the greatest use in tracing the
lower limestone through the district. The same likewise appears in Ohio in equal abundance.
In the Third District this group is much more extensively developed than in the Fourth, and
its products are even more variable. Its most obvious fossils are marine plants, or Fucoids,
which everywhere mark its shales and shaly sandstones; but in the Fourth District, rarely
more than one species is seen, and this is common in the thin layers of sandy shale succeeding
the lower green shale. This species closely resembles one in the Hudson river group, and
bboth ear much analogy to the F. antiquus as figured by Hisinger. The following figure
is from a nearly perfect specimen as usually seen, and it may be considered the lowest fossil
of the group on the Genesee river.
CLINTON GROUP. 69
==EE
# =#
=#E=# Ej ===
= E \;
*===#74; Hé.
E===
| s==
ºsº
|)
| 2.
zºº
:=>*=-
Hº
Nº
sº
===
#==\º
== Ez
A=
Aftā
*==
ºº:: -
tºº - -
º: &"º º º ** **, rºº L. g., e Azazzº º-º-º-º-
º, ºf }% %.º.2.5.22.2 2%ZZZZZºº
Fucoides Gracilis.
This species is one of the most delicate of the marine plants preserved in our rocks, and
the specific name of gracilis is proposed. The branches sometimes appear as if nodulose or
vesicular. The specimen figured is probably only a branch from a larger individual. It will
be observed that the stem and lateral branches are of equal size; it was therefore a floating
and probably a flexible plant, as the stem could not have supported branches of its own di-
mensions. This species beautifully contrasts with the strong and rigid forms from the same
group farther east.
In the Fourth District, the lower limestone, as its name implies, is eminently characterized
by the presence of the Pentamerus oblongus of Murchison. This fossil exhibits a great variety
of form as well as of size. The shells are nearly all broken, and so packed together as to
indicate that they have been drifted by a current or washed by the waves, while the mass
formed the margin of the ocean or an elevated portion of its bed. At Rochester they become
an entire layer of about one foot in thickness, but farther east they are distributed throughout
the whole rock, and bear evidence of much wearing before being imbedded; they are also
frequently much intermixed with green shaly matter.
The following woodcut gives illustrations of some of the common forms.
70 GEOLOGY OF THE FOURTH DISTRICT.
*
£3: -
º º
*
1 – 5. Pentamerus oblongus. ‘. 6, Delthyris brachynota.
Pentamerus oblongus. – Fig. 1 is a view of the larger valve of a full grown individual,
showing a great expansion toward the base, and a tendency to a three-lobed character. The
concentric lines of growth are strongly marked.
Fig. 2 is the smaller valve of a younger shell, which presents a more circular form, but
still the same tendency to trilobation. -
Fig. 3 is a side view of a perfect specimen, showing an intermediate proportion between
the others. $
Figs. 4 and 5 are casts of the upper and lower valve, showing those divisions upon which
the generic character depends.
The Pentamerus commences in the Third District, and from its prominent characters fur-
nishes a good guide to the existence of the group as far west as the Genesee river. It some-
times occurs in the iron ore both in the Third and Fourth Districts.
This fossil is typical of the calcareous beds in the Caradoc sandstone of England, and
specimens of the mass with broken shells from the Hollies, can scarcely be distinguished
from those on the Genesee and in Wayne county. Mr. Murchison has described two species,
the P. laevis and P. oblongus, both of which appear to be represented in our numerous varie-
ties, and are apparently referable to the same shell.
CLINTON GROUP. 71
I have obtained beautiful casts of this fossil in a light grey limestone (lower part of the
“cliff,”) from Springfield and Dayton, Ohio, and have seen them from several localities in
Indiana. In Iowa I collected some fine silicified casts of the same, from the cliff limestone,
on the Maquoqueta creek. It is therefore a widely distributed fossil, and when more
thoroughly examined will doubtless be found typical of certain strata at the west, as in New-
York. t -
Fig. 6, the Delthyris brachynota accompanies the Pentamerus, and even continues long
after that fossil has disappeared; several specimens having been seen near Reynolds’ basin,
in Niagara county. It is the only Delthyris known in this rock, and is readily recognized by
the relatively short hinge line.
The other fossils of the limestone are represented in the following woodcut:
16.
1. Orthis circulus. 3. Atrypa naviformis.
2. Atrypa congesta. - 4. Atrypa plicatula.
5. Crinoidal joint. (Natural size and magnified.)
1. Orthis circulus.-This is a beautiful, circular, finely radiated shell, with a narrow area.
It is found accompanying the Atrypa congesta at Reynolds' basin. It is distinguished from
a similar shell in the Hamilton group by its greater length on the hinge line, and the greater
proportional width of the shell. -
2. Atrypa congesta (of Conrad). —West of the Genesee river, after the disappearance of
the Pentamerus, we find the lower limestone of the group distinctly marked by the presence
of this small Atrypa, which is exceedingly abundant at Medina, and near Reynolds' basin.
It is associated with the crinoidal joints like fig. 5 of woodcut. It appears standing out in
relief upon the surface of weathered specimens, which are abundantly strewed over the ground
a mile or two south of Medina. Near Reynolds’ basin it occurs in great numbers, completely
covering the surface of certain layers, and large numbers of separate individuals can be
obtained among the decomposed portions. This shell appears to take the place of the Pen-
tamerus so far as regards numbers of individuals, prominence, and place in the strata.
It is a smooth shell closely resembling Atrypa linguifera of Murchison's Silurian System,
pl. 13, fig. 8; but the length of the latter appears to be greater in proportion, and the shell
72 - GEOLOGY OF THE FOURTH DISTRICT.
smaller; the mesial elevation of the upper valve also appears more prominent, judging from
the figure. This shell occurs in the iron ore bed at Rochester. - -
3. The Atrypa naviformis is a nearly globular smooth shell, the beak extending considerably,
and incurved; the lower valve is much elevated in front, after the manner of A. linguifera
and A. congesta. This shell is typical of the upper limestone of the group, and so far as I.
know, is found in no other rock.
4. The Atrypa plicatula presents three of the folds raised in front, and from six to eight
on either side; three of them very distinct, the remaining ones obscure. There is a slight
depression in the upper valve, extending from the beak one-third the length of the shell.
5. Joints or plates of Actinocrinus 2 plumosus. – This fossil is found in greater or less
profusion in the lower limestone, throughout the extent of the district. It appears in great
numbers one mile south of Medina, in the weathered specimens of the rock. Large surfaces
are often covered with them, usually presenting the form given in the illustration. A mile
west of Reynolds’ basin they are equally abundant, associated with the Atrypa congesta and
A. plicatula.
With the crinoidal joint are found some plumose tentaculae of a crinoid, which apparently
belong to the same species. It is provisionally placed in the genus Actinocrinus, and this
character of the tentaculae gives its specific name. --
In the green shale we find, for the most part, a different association of fossils from those
of the limestones, though two or three species are common to both. In the accompanying
illustration are presented the most common forms found in both the upper and lower green
shale.
17.
º
#%; §§ :
& ſº sº §:
% §§§º §§
ºfºliº
/º º º
& §§§§ſ:
º
º : tºº
º º
º º tº. §§
º § §§ º: &
& % - #: §§
--> ſº ~ - º º
º º º: º
jº º - §§ ś ºº::
33 º §§ tºș
º §§§ iº § ºš:$ º sº
f * º §§
6 º ºš'
º 3. º §§§ sº
º º §§
§º ºğ
º §§§ º
& §
& # º § t § §§
(ºff º |#AW º º §§
U &
1. Strophomema elegantula. 7. Posidonia? alata.
2. S. corrugata. 8. Atrypa affinis? var?
3. S. cornuta. 8a. — — (young shell).
4. Atrypa hemispherica. 9. Calymene 7 trisulcata. -
5. Littorina cancellata (young shell.) 10, Agnostus latus, natural size and magnified.
6. Tittorina cancellata (old shell). 11. Tentaculites minutus, natural size and magnified.
12. Graptolites Clintonensis.
CLINTON GROUP, 73
All the specimens here figured occur in the upper green shale, and nearly all at Rochester.
Figs. 5, 6, 8 and 8 a, occur in the lower green shale in Wayne county, being common to
the two shales. -
1. Strophomena elegantula. — This is a beautiful semicircular shell, marked with strong
elevated lines, having from four to six fine striae between each. It occurs in Wayne county,
and at Rochester. This shell bears considerable resemblance to S. transversalis.
2. Strophomena corrugata. (Jour. Acad. Nat. Science, Vol. viii, p. 256, Pl. 14, fig.
8.)—This shell is beautifully radiated, the rays dividing, a larger and smaller one alter-
nating. On the hinge margin it is marked with a few oblique folds, which are frequently
obsolete in well preserved specimens. This appears to be the fossil of which large numbers
are imbedded, and completely silicified in the Pentamerus limestone. It occurs both in the
limestone and shale. The specimen figured is from the upper green shale at Rochester.
3. Strophomena cornuta. — Shell semicircular, finely and equally striated; hinge line
straight; each valve furnished with six small, stiff, diverging spines. This shell closely resem-
bles the Leptana lata of Von Buch, as figured in the Silurian System (Pl. 5, fig. 13); but
it is much smaller, and apparently more finely striated. The L. lata is found in the Ludlow
rocks of England, which are equivalent to our Hamilton group. The S. cornuta occurs in
a situation associated with fossils typical of the Caradoc sandstone of the Silurian System.
This shell is abundant in the upper green shale at Sodus bay. •.
4. Atrypa hemispherica (?) (Silurian System, Pl. 20, fig. 7). — This little shell has from
twelve to fourteen radii. It is usually much flattened, though one valve is much more convex
than the other. It corresponds very closely with the figure and description given by Mr.
Murchison. It occurs in such numbers in the upper green shale at Rochester, as to form
two thin layers before referred to, where the shells retain their natural pearly lustre. This
fossil occurs at Wolcott, Sodus, Rochester and Medina, as well as several other places.
5 and 6. Littorina cancellata. — Fig. 5 is a young individual of this species, finely and
beautifully cancellated over the whole surface. This marking is prominent in young speci-
mens, but becomes obliterated in older ones, as is seen in fig. 6, where two views are given of
an older individual of the same species. Some faint longitudinal striae are here visible, and in
other specimens I have detected the crossbarred markings partially worn off. The shell is
frequently quite smooth. It is abundant in the green shale at Sodus, and at Rochester; also
in the Pentamerus rock at Rochester and Medina.
7. Posidonia 2 alata. — Shell compressed, alated behind and rounded before, very inequi-
lateral, wider than long; surface rather strongly marked with concentric lines of growth.
Found in the upper green shale at Rochester. It is not an abundant fossil.
8. Atrypa affinis, var. 2 – This shell presents the form and markings of some of the indi-
viduals referred to that protean species. The portion within the shaded line is strongly ribbed
and marked by lines of growth ; without this line, the margin is compressed, and the lines of
growth scarcely defined. It often occurs, presenting this form, and appears like the A. affinis
surrounded by a fringe. -
GEOL. 4TH DIST. 10
74 - GEOLOGY OF THE FOURTH DISTRICT.
Fig. 8 a, is apparently a young individual of the same species. It so frequently occurs of
this oblique form, that I have presented a figure.
This shell is abundant in the upper and lower green shale at Wolcott, Sodus and other
places in Wayne county, and less common at Rochester and the localities at the west. A
similar form, however, is abundant in the upper part of the limestone of this group at Lock-
port, the variation perhaps due to the nature of the matrix. This, or another variety is
abundant in rocks of this group in the Third District, and considered among its disinctive
fossils. -
9. Calymene 2 trisulcata. — This little Trilobite is one of the fossils occurring in the
green shale at Rochester, associated with those here described. Body with eleven articula-
tions; tail with four distinct articulations on each lateral lobe, and six on the central one ; the
central lobe of the head is marked on each side by three indentations or furrows, which ex-
tend about one-third across it. In these furrows it somewhat resembles the Triarthrus,
and more nearly the Calymene? Downingia, of the Wenlock limestone.” The structure and
arrangment of the eyes, however, differ from the latter; and according to the strict definition
of the genus Calymene, it should be separated. Our specimen is much smaller than C.
Downingia, its length being but half an inch.
10. Agnostus latus. – Natural size, and magnified. This fossil is placed among crustaceans
by naturalists. It usually presents two views: one with a narrow depression in the centre
and an elevation on each side, and flanked by an expanded border; another form where there
is only a slight broader depression in the centre, and no elevated ridges — probably the two *-
sides of the creature. This fossil occurs in great numbers in the upper green shale at
Rochester, and also at other localities. In the Third District it occurs in millions, and though
so small, yet constitutes a large proportion of some thin Sandy and shaly layers in rocks of
this group south of Utica. - - -
This is the lowest position in which this fossil is known in New-York. It was discovered
in the green shale at Rochester, in the second year of the survey; and since that time, it
has been found in many other localities. .”
11. Tentaculites minutus. – This fossil occurs with the Agnostus and other forms in the
green shale at Rochester. The figures are of the natural size, and magnified. It is dis-
tinctly annulated near the base, but apparently smooth above. Its minuteness, and the
compressed and flattened form in the shale, renders a full examination of the specimen dif-
ficult. -
12. Graptolites Clintonensis. – This fossil occurs in great abundance in the upper green
shale at Sodus, Williamson, Rochester, and numerous intermediate points. The serrae or
teeth are usually long, and bent or recurved, though others associated with them differ in this
respect. I have not yet decided whether one or two species exist. At Sodus the shaly
laminae are completely covered with these bodies, broken into short fragments, and lying in
great confusion; more perfect specimens are often found with Strophomena cornuta. In the
* Silurian System, p. 655, pl. 14, fig. 3.
CLINTON GROUP. - 75
eastern part of Williamson, a little north of the Ridge road, the shale is completely charged
with them, and very black and brittle, as if from carbonaceous matter derived from the fossil.
The same character of the slate containing them, is noticed on the Genesee. This fact, and
other similar ones, together with the carbonaceous nature of the fossil, would argue against
placing these bodies among the calcareous polyparia. The specimen figured, resembles in
some degree the G. Ludensis (Silurian System, Pl. 26, figs. 1 and 2); but in ours the serra
are longer, less closely arranged, and the whole individual more delicate. Since also this
fossil is found in rocks much lower than the Ludlow rocks of England, the probability of its
being a distinct species is increased, and a specific name indicating its position is given.
The shale associated with the iron ore at the Wolcott ore bed, though apparently holding the
place of the upper green shale, contains an assemblage of fossils mostly different from those
of that rock in other places, and also differing from those of the group generally in the Fourth
District. Several other forms occur besides those presented in the following illustration, all
differing as much from the ordinary ones; while at the same time no fossil was found asso-
ciated with them, which is common to the group elsewhere. This circumstance, however,
adds but another fact to the many, regarding the geographical distribution of fossils in this
group, and proving that upon the lithological character of the products depended, in a great
degree, the organic forms which inhabited the bed of the ocean. -
An exhibition of the lithological development of the Clinton group at different points along
its range, together with the fossils of each division, furnishes an instructive illustration of the
nature and products of geological formations. We have here changes in the space of two
hundred miles, as great as in other formations, when traced over an extent of as many thou-
sands. The two extremities of the group within the State present scarcely any features in
common, either fossil or lithological. -
While this group contains an assemblage of fossils peculiar to itself, and marking it as
clearly as other formations are distinguished by similar characters, a few forms link it with
the next group in the ascending order. The Strophomena depressa appears here as its lowest
position, and continues through several succeeding rocks. The Delthyris radiatus, and a
smooth species of Atrypa, are also common to this group and the Niagara, not appearing in
any higher position. The Catenipora escharoides, which is abundant in the upper part of
the Niagara, first appears in this group. º -
The forms presented in the illustration No. 18, are from the shale of the Wolcott ore bed.
76 GEOLOGY OF THE FOURTH DISTRICT.
18.
1 Orthomota curta. 4. Nucula mactræformis. 7. Lingula elliptica.
2. Nucula machaeriformis. 5. Avicula leptonota. - 8. Lingula oblata.
3. Cypricardia obsoleta. 6. Cypricardia? angusta. 9. Lingula acutirostra.
1. Orthonota curta. —Length rather more than twice the height of the shell; posterior
slope obtusely carinated. This shell is readily known by its straight hinge line, truncated
posterior margin, and numerous plications extending from the oblique fold or keel to the an-
terior margin. The characters of the genus, as given by Mr. Conrad, are perfectly applicable
to this shell. One specimen has been found at Rochester, which is the only one, with the
exception of those at the ore bed.
2. Nucula macha’riformis. – The shell is much elongated, and faintly marked with con-
centric striae; beaks scarcely prominent. The elongated form, and scarcely visible striae,
distinguish this shell from all others of the group. It is always much flattened from pressure,
and was apparently a fragile shell. It resembles Machaºra (Solecurtus) costata in form ;
and in some specimens, I have seen impressions of a rib extending from the beak, as in that
shell.
3. Cypricardia obsoleta. — Beaks very prominent; shell marked with faint lines or folds,
scarcely striated. Its prominent beaks and rhomboidal form, with the worn or decayed ap-
pearance of the shell, are its distinguishing marks.
4. Nucula mactra formis.-Shell ovate, marked by concentric striae which are stronger
upon the anterior margin; a slight fold (perhaps from compression) extends along the posterior
slope. Height two-thirds the length of the shell. The form and proportions of this shell
distinguish it readily from others of the group. -
5. Avicula leptonota. — This shell is usually marked by strong longitudinal ribs, and
crossed by fainter concentric lines; posterior hinge margin depressed. In many specimens
the concentric lines are nearly obliterated, and the longitudinal ribs only visible. It occurs
in considerable numbers, often crushed, and its form nearly destroyed.
6. Cypricardia 2 angusta. — Shell narrow, much elongated, marked by concentric folds
which are more prominent and fewer in number on the anterior margin. The hinge resembles
externally the Cypricardia, but the internal arrangement cannot be seen.
CLINTON GROUP. 77
7. Lingula elliptica. — Shell oval, nearly equal in width at each extremity, marked by
concentric lines or slight folds, which are scarcely elevated. -
8. Lingula oblata. — Shell very wide in proportion to the length; surface marked by con-
centric lines or slight folds, which are stronger and more prominent on the margins; the whole
surface covered with exceedingly fine concentric striae. This shell differs from the last in its
proportions, and in having two series of concentric markings which do not appear in the first.
9. Lingula acutirostra. —This shell is readily distinguished from the other two by its
form, and also from any described Lingula of the New-York rocks. The shell is broad be-
low, tending abruptly to an acute point at the apex; surface marked with a single series of
rather coarse striae. It is larger than the L. acuminata, and the surface more strongly marked
by the concentric striae, as well as more abruptly acute. -
The three species here described are all found in a single locality, the two last quite nu-
merous. This circumstance is somewhat unusual; the shells of this genus, though often
abundant, rarely exhibit more than a single species in a rock or at a locality.
All the forms presented above, with several others, may be obtained in the shale at the
Wolcott ore bed, and those of the previous illustration at Sodus point and Rochester; while
Medina and Reynolds's basin will afford a rich harvest in the other forms, as well as some
not described. - º
The following woodcut is an illustration of the characteristic fossils of this group in the
Third District, and is from Mr. Wanuxem's Report. -
19.
ſº
É
*
º
lift
º º
º
Š É.
šá%
l. Fucoides biloba. 3. Crinoidal joint. 5. Strophomena depressa.
2. Tail of Hemicrypturus. 4. Lingula oblonga. e
The Strophomena depressa, and tail of Hemicrypturus, are the only fossils of this illustra-
tion which are found in this group in the Fourth District, and they are by no means common.
78 GEOLOGY OF THE FOURTH DISTRICT.
The other forms have never been met with, though they are abundant farther east. The
Lingula oblonga is distinguished from either of those just described, by its straight parallel
sides and abruptly rounded base, and also by a series of longitudinal striae, not seen in either
of the others.
t
Sections illustrative of the order of succession among the members of the Clinton group, and
7ts connection with the rocks above and below.
These sections illustrate the connection of the Clinton group with the overlying and under-
lying rocks, and also show its variations in character and development at different points in
the district. The same order of the strata, and nearly the same degree of development, occur
in the eastern part of the district, as that exhibited in the section on the Genesee. The sec-
tions of this part are omitted, as not showing, in the same conclusive manner, the connection
of the group with those above and below.
20.
4-
-
º
#
£2
#
#
f
J.
º *-
*-
==
š
:= <
* Sºº-
Section on the Genesee river, from the upper to the lower fall at Rochester.
1, 2, 3. Upper, Middle and Lower falls.
g. Shale of Niagara group.
( f, Upper limestone of Clinton group.
CLINTON GROUP. e. Upper green shale.
d. Pentamerus limestone.
U c. Lower green shale.
b. Grey band, upper part of Medina sandstone.
a. Medina sandstone. - - - - §
The section (No. 20) exhibits the order of superposition in the strata forming the Clinton
group, a part of the Medina sandstone, and the lower part of the Niagara group. In the
banks of the Genesee, this order of succession is as clearly seen as in the woodcut. The
green shale rests directly upon the upper part of the Medina sandstone, and extending beneath
the Pentamerus limestone, forms, together with that rock, the Middle fall, twenty-five feet.
The limestone, however, is the resisting stratum, and about one half the lower part of the
shale forms a slope extending towards the Lower fall. * - -
Above the Pentamerus limestone, the upper green shale forms the bed of the river nearly
to the Upper fall, the limestone above producing rapids in the stream for a short distance.
The whole height of the upper fall is over the shale and lower beds of impure limestone of
the Niagara group. + -
CLINTON GROUP. 79
1. Section of the strata one mile south of Medina. 2. Section showing the Clinton group and associated
- - strata at Lewision, on the Niagara river.
g. Niagara shale. - -
f. Upper limestone of Clinton group. e Niagara shale.
e. Place of the upper green shale; no rock seen. d. Limestone, formed by the junction of the lower and
d. Pentamerus, or Lower limestone of Clinton group. *. upper limestones of the group.
c. Lower green shale of Clinton group. c. Lower green shale of Clinton group.
b. Terminal grey mass of the Medina sandstone. b. Terminating grey portion of the Medina sandstone.
a. Medina sandstone. a. Medina sandstone.
&
Section 1 illustrates the order of succession one mile south of Medina, where the lower
green shale of the group has diminished to three feet, and there is no evidence of the upper
green shale, although the absolute contact of the limestones is not seen. The two limestones
preserve nearly the same characters as at Rochester, though there is more hornstone in the
lower mass, and its typical fossils are absent. - -
The upper limestone contains pyrites, and is often iron-stained, presenting numerous irre-
gular cavities. It also contains its peculiar fossil, Atrypa naviformis. The shale of the next
group follows in the same order as at Rochester. -
Section 2 illustrates the order of succession among the strata at Lewiston, and along the
Niagara river the same order is preserved. There is little change from Medina to this point,
except that the two limestones of the group are here not only in contact, but apparently form
a single mass, the lower part differing somewhat from the upper. -
80 GEOILOGY OF THE FOURTH DISTRICT.
Wiew of Niagara Falls from the Canada shore, From a drawing by Mrs. HALL.
11. NIAGARA GROUP.
Geodiferous limerock, and Calciferous slate, of EATON. Lockport limestone, and Rochester
shale, of the Annual Reports of the Fourth District. Upper part of the Protean group,
of the Annual Reports of the Third District.
(A PART of No. 6, IF REcognizED, IN THE PENNSYLVANIA SURVEy.)
[See Section of Niagara River from Lewiston to the Falls, Plate 3; and L. l. of woodcut, p.27.]
This group consists of two distinct members, a shale and limestone, which, possessing
many features in common, are recognized as the products of one period; during which, how-
ever, there was an important change in the lithological products, and a less one in the organic
forms. The shale continues a very uniform deposit throughout the whole extent of the dis-
trict; while the limestone, from a thin, dark-colored concretionary mass, becomes an extensive
and conspicuous rock, constantly increasing in thickness in a westerly direction, even far
beyond the limits of the State.
The Cataract of Niagara is produced by the passage of the river over this limestone and
shale; and from being a well known and extremely interesting point, as well as exhibiting the
greatest natural development of these rocks within the limits of the State, this name is adopted
for its designation.
NIAGARA GROUP. 81
The members of this group are:–
1. Argillaceous, or (in many localities) argillo-calcareous shale.
2. Limestone, presenting several different varieties.
1. NIAGARA SHALE.
The lower part of the Niagara group exhibits a great development of dark, bluish shale,
which on exposure gradually changes to grey or ashen color, and forms a bluish or greyish
marly clay. In this state, it is undistinguishable from the ordinary clays; and its outcropping
edges, where long weathered, are often considered as clay beds. This character is well ex-
hibited at Lockport, on the northern slope of the terrace where the canal and railroad have
been excavated; and also at numerous localities in Wayne and Monroe counties. The depth
of tint in the clay differs according to degree of exposure, the outer portions becoming of the
usual yellowish brown color of the ordinary soils.
When freshly excavated, the mass is tough, and breaks irregularly, some portions only
exhibiting a slight tendency to slaty structure. After weathering for a short time, it cracks
in all directions, and soon falls into innumerable angular fragments, when the disintegration
goes on till it forms the soft clay. This change seems due to the intimate mixture and de-
composition of iron pyrites in the rock; and its presence is also indicated by the production of
sulphate of alumina, on decomposition in favorable situations, and upon calcination. In color,
aspect, manner of weathering, and other properties, it closely resembles the shale of the upper
part of the Hamilton group in the Fourth District. Neither are micaceous, and both are
slightly calcareous, probably from the great amount of organic matter. The Niagara shale,
however, is destitute of those spheroidal concretions, which in the Hamilton group are more
or less common, and in many places abundant. The only approach to a concretionary form
seen in this shale, is in the increased thickness of some layers of impure limestone; and this
appears rather due to a greater development of corals or other fossils, around which the mud
accumulated more freely than elsewhere. A few such examples may be seen in the banks of
the Genesee at Rochester.
The lower part of this shale is mostly free from calcareous bands; while towards the middle
and in the upper part, we find numerous thin, wedge-form or continuous layers of impure
limestone, mostly composed of corals and other fossils, and their surfaces covered with the
same, forming beautiful and interesting specimens for the cabinet. The perfect similarity of
these with specimens from Dudley in England, together with the identity of many of the
organic forms, renders the conclusion unavoidable that the two are formations of the same
age. These layers are from half an inch to two inches thick; and from the decomposition
and sinking down of the shale, they are usually found broken into fragments. One of the
most striking features of this rock is the abundance of its fossils, which will be enumerated
in another place. Scarcely a locality can be examined where they do not occur in great
perfection.
GEOL. 4TH DIST. 11
82 GEOLOGY OF THE FOURTH DISTRICT.
The higher beds are well developed in the falls at Wolcott village, and the lower part of
the formation can be examined by following down the ravine for a mile. This is the most
eastern locality in the district where we find the rock exposed. West of this point, through-
out the county, it is seen in all the small streams which flow into the lake.
jº
º º
§NºS §§ :
§§ §§§ ɺ:
§§ ºß
sº º
§§ §§§ { | #| ||
Sººn iº. § lº
§: | tº: tº * # 2* º
$$. &
º
* . sº
|jº
* z º.º.
#ftº:
§§§
§s * -
44.292
&
złºrs A,
View of the Upper Falls at Rochester.
At Rochester it forms nearly the whole height of the upper fall, and the banks on either
side of the river for more than a mile below. This place offers a fine exhibition of the rock,
and is one of the best localities in the State for a natural exposure. The constant undermining
of the banks precipitates large masses to the bottom, and their fossil contents are thus made
accessible. At this locality, its upper and lower limits are both plainly seen. Above it passes
gradually into an impure limestone, which forms the beds of passage from the shale to the
limestone above. The fossils mostly disappear at this point, and few are found in this part
of the mass. Below it terminates abruptly, resting directly on the calcareous beds forming
the upper member of the preceding group. There is never any gradual passage from the one
to the other, and the peculiar fossils of the shale do not appear till we ascend some distance
above the limestone. Nevertheless it is true that two or three of the common fossils of this
shale have been found in the limestone below, and at the same time the greater number marking
the Clinton group terminate below that rock. It may therefore remain a question, perhaps,
whether these calcareous beds should be included in the Niagara group. Since, however,
they bear a close analogy to the lower limestone of the Clinton group and terminate above
abruptly without offering any marks of gradual passage to the next higher group, I prefer for
the present to include them in the lower, thus presenting a natural lithological assemblage.
The presence of a few fossils common to the limestone and shale above would apply equally
to all parts of the preceding group, a few forms being common to all parts of both.
The precise arrangement at Rochester is as follows:—The terminating calcareous beds of
the Clinton group consist of fifteen or twenty thin courses, each separated by a layer of shale,
NIAGARA GROUP. 83
sometimes of equal thickness to the limestone, though generally thinner. The shale sepa-
rating the lower courses is green like that below; but higher, it becomes of the same color
and character as that above. The interlaminated shale is in all cases destitute of fossils.
The shale is partially exposed in several small streams, and in the low escarpment which
extends westward from Rochester. In the town of Sweden, that escarpment has become
higher, and the shale is in some places well exhibited. One of the best localities is at Mar-
shall's saw-mill, in the town before mentioned, where the small stream (a branch of Salmon
creek) has excavated its channel in this rock. The banks scarcely differ in color and ap-
pearance from the soil around, and it is only from fossils that the mass is distinguished from
ordinary clay. At one point where there has been a fresh exposure, the rock appears in all
its characters, and contains abundance of fossils.
Passing westward from Monroe county, the escarpment constantly rises, and the shale .
appears in all the ravines and water-courses; and the smallest gorge is often sufficient to
afford a good exposure of the rock, which is every where charged with fossils. Even in the
banks of ditches, passing through some level grounds, I have obtained many fine specimens
from the decomposed portions. -
Below Farwell’s mills in the town of Clarendon, and again on the south side of Jefferson
lake, and along the escarpment between this and Albion, the shale is exposed in many places,
and in all yields abundance of its organic remains, which appear to increase in number to-
wards the west. - -
At Shelby falls, the upper part of the shale, and the siliceous limestone terminating it, both
appear; and the former continues in view for a mile north of this point, in the banks of the
stream. Thence to Lockport, the rock may be every where examined along the northern
slope of the Great Terrace, except in places where there has been too great an accumulation
of drift. -
At Lockport, both from natural exposure, and from artificial excavations in the construction
and enlargement of the Erie canal, this rock in all its varieties is better exhibited than else-
where west of the Genesee. The banks of the natural gorge where the canal enters the
escarpment, appear like immense beds of clay surmounted by limestone. The effect of de-
composition has been such as to obscure the natural color and appearance of the mass. Along
the sloping sides of these apparent clay banks we find vast numbers of the peculiar fossils of
the rock, and every excavation adds a fresh supply to the almost exhaustless numbers. The
shells, being purely calcareous, resist the effects of decomposition; while the mass around
crumbles down, leaving them in a perfect condition, and entirely separate from the matrix.
Between Lockport and the Niagara river, the shale appears in numerous ravines and gorges
which indent the edge of the great escarpment. The whole thickness of the shale is exposed
in both banks of the Niagara, extending from Lewiston and Queenston to the Falls. From
difficulty of access, however, it does not afford so good an opportunity of investigation as at
Lockport and Rochester. At the points where I have been able to examine it, it retains the
same characters and affords the same fossils as at localities farther east. Along a part of the
distance, it is partially obscured by fallen fragments of the limestone which caps the cliff.
ź
84 GEOLOGY OF THE FOURTH DISTRICT,
2. NIAGARA LIMESTONE.
A silico-argillaceous limestone forms the beds of passage from the soft shale below, to the
purer limestone above. When freshly exposed, it is often of a dark or bluish color, but soon
changes to light grey or ashen; and though variable in character, it is a constant accompani-
ment of the group as far as observed. It forms a good hydraulic cement, where it has been
used for that purpose.
In the eastern part of the district, these beds of passage are succeeded by a dark bluish
grey, subcrystalline limestone, of a rough fracture, and separated into thin courses by dark
shaly matter. When not too much divided by seams, it forms a durable building material.
This, again, is succeeded by a coarse-grained concretionary mass in irregular layers, exhibiting
an appearance as if much disturbed while in a semi-fluid or yielding condition. The concre-
tions often present cavities lined with crystals, or the remains of some fossil body. The upper
strata are finer grained, with a resinous lustre; and on weathering, the surface is harsh and
sandy to the touch; this, however, seems due to the presence of magnesia rather than silex.
In the western part of Monroe county, the hydraulic layers are succeeded by a light co-
lored and very porous encrinital limestone; which, farther west, becomes the compact crinoidal
limestone of Lockport.
In the western part of the district, this crinoidal mass is succeeded by a light grey limestone
with cavities, and containing many corals. Above is a darker colored mass, still with cavities
lined with crystals of spar; and the series is terminated by a thin-bedded concretionary lime-
stone, strongly bituminous, the layers separated by shining black carbonaceous shale.
This rock first appears in the district at Roe's quarry in the town of Butler, Wayne county,
where the hydraulic layers are not seen, and the rock has the character of a dark blue lime-
stone, very fine-grained and compact, yielding a bituminous odor on percussion. It is mostly
thin-bedded, and exhibits little tendency to a concretionary structure, being readily quarried,
and furnishing a good building material where heavy blocks are not required; its principal
use, however, is for burning to lime. Farther west the rock outcrops by the roadside, but has
not been quarried. It here exhibits the dark greyish color of the higher strata. -
This limestone is likewise quarried at Henderson's in the same town, exhibiting a thick-
bedded structure, and regular stratification.
It again appears in the town of Rose, at Uttoe's or Miner's quarry, on the head waters of
Sheldon's creek. At this place it is thicker bedded than farther east, appearing in courses of
two or three feet, having a dark color and granular texture.
It has been quarried at two places on the line of the Sodus canal, where it presents ap-
pearances similar to those just mentioned. It is also exposed in the towns of Marion and
Walworth, passing thence into Monroe county. The whole length of its outcrop in Wayne
county is marked by a range of limekilns, which always indicate the proximity of the rock.
The variations which it undergoes in this distance are principally an increase in thickness,
and a gradual change to a lighter color in the central portions of the mass. Its concretionary
NIAGARA GROUP. 85
structure is not often well exposed, though it does appear in a few of the strata. Cavities
or geodes, lined with calcareous spar, gypsum, etc., are occasionally found, and there is a
constant increase of their number and size in a western direction. .
The lower part of this limestone, possessing a siliceous character and properties of the
hydraulic cement, occurs in the towns of Rose and Williamson. -
In Monroe county, the northern margin or outcropping edge of this limestone extends through
the towns of Penfield, Brighton, Gates, Ogden and Sweden; in each of these places, nu-
merous localities are presented for its examination. The principal outcropping portion is the
dark grey upper mass, which is highly bituminous, and when weathered has a harsh feel like
a friable sandstone. On fresh fracture, it is often dark blue, or approaching to black. It
appears to be composed of Small crystalline grains, which present numerous shining lamina:
of a resinous lustre; and the rock, from its aspect, often resembles a sandstone rather than a
limestone. It every where furnishes a good lime, but of a yellowish color. Large quantities
of bituminous matter are expelled in the process of burning; and this substance frequently
flows from the kiln, of the consistence of tar. The rock, on examination, proves to contain
no appreciable amount of silex, but is every where magnesian; and it is probably from the
mixture of the two earths that the harsh or siliceous-like character is presented. Exposed
fragments are often quite porous, from the solution and removal of a portion of the matter.
Its northern limit, through the eastern part of Monroe county, is marked by an accumulation
of fragments of the rock, which are rounded rather from weathering in place than from trans-
portation. These always exhibit on their outer surfaces the peculiar porous or spongy texture.
That their form and decomposition is due to weathering in the places we find them, is evident
from the frequent presence of some silicified fossil which stands out upon the surface in strong
relief. In many places this stone is exceedingly brittle, particularly on first exposure.
At the Penfield mills on the Irondequoit, the lower part of the limestone appears in the bed
of the stream, and underlies the surface at no great depth for some distance around. It is of
a bluish color, very hard and tough, mostly thin-bedded, and separated by seams of shale. In
consequence of its hardness, it is rejected as a building stone, and quarries are sought at a.
greater distance. {
At Rochester, the lower beds have the same siliceous character as farther east. They pass
upward into a coarsely granular or compact subcrystalline limestone, very irregularly stratified,
and the layers separated by greenish shale. The strata are often wedge-form, or irregular in
thickness. This portion of the rock is partially composed of fragments of crinoidal stems and
other fossils, but so comminuted that their forms are usually undistinguishable.
Still above this, the rock which forms the central portion of the mass presents itself in very
irregular concretionary or contorted strata. The whole exhibits an appearance as of folding
among the laminae, by which it has partially assumed the form of spheroidal concretions, but
still inseparable from the adjoining and surrounding rock, which may be only partially folded
or contorted, and connecting this with another spheroidal mass. A very similar example, on
a small scale, may often be seen in a very curled and gnarled plank or stick of timber.
86 GEOLOGY OF THE FOURTH DISTRICT.
Concretionary and contorted Strata, Rochester.
This portion of the rock, as it appears in the vicinity of Rochester, is grey and subcrystal-
line, very hard and tough, exceedingly irregular in its stratification, and difficult to quarry.
Sometimes for a short distance the strata are regular, and then separated by seams of shale,
and again all trace of stratification is lost, and the whole assumes the contorted and concre-
tionary structure. It contains numerous cavities partially filled with crystalline materials,
such as dogtooth and rhomb spar, gypsum, and more rarely sulphate of strontian and the sul-
phurets of lead and zinc. In many instances, these cavities present a partially decomposed
organic body, as a Favosite or some other coral, which seems to have formed the nucleus
around which the stony matter accumulated. Sometimes the remains of these are distinctly
visible; at others, they are entirely obliterated, the form of the cavity being the only evidence
of their having existed. -
In the accompanying illustration, which represents the remains of a Porites, the transverse
laminae, indicating the stages of growth in the coral, are distinctly preserved, while all the
intermediate parts are removed, only a few calcareous crystals remaining in the spaces.
The succeeding portion of the rock, here as elsewhere, is of a grey or greyish brown color,
often darker on first exposure, but always weathering to the grey shapeless masses, seen
. NIAGARA GROUP. 87
abundantly scattered over the surface. This part likewise exhibits numerous irregular cavi-
ties, with calcareous spar and fluate of lime, and blende is more frequently found here than
below. Nodules or accretions of light-colored brittle hornstone occur every where; and the
fossils are often silicified, and stand out in relief upon the surface. The Catenipora escha-
roides marks this part of the rock, though it is often nearly destroyed or absorbed; still, a
careful examination will enable one to detect it, and in more favorable situations fine speci-
mens are obtained. It is this part of the rock which appears at the rapids on the Genesee
above Rochester, and elsewhere both on the east and west sides of the river. There are
usually some thin-bedded regular strata above this, which are mostly used for burning to lime;
the concretionary and irregularly stratified portions of the central division being too impure,
and too difficult to be quarried for this purpose. The upper strata are not only readily quar-
ried, but are easily broken into fragments of suitable sizes. It breaks with a dull sound, and
presents a slightly uneven fracture. *
The lithological characters alone of the two upper divisions are every where sufficient to
distinguish this part of the rock from all other limestones in the State; these are, its brittle
nature, the glistening surface of the minute crystalline laminae of which the mass is com
posed, and its harsh or apparently siliceous character.
The characters, as described at Rochester, are the prevailing ones, for a great distance
westward. The dark-colored mass, however, above the beds of passage or hydraulic lime-
stone, thins out, and its place is occupied by a light grey crinoidal limestone, sometimes
composed of extremely comminuted particles, at others exhibiting portions of the crinoidal
columns and other fossils.
The following arrangement will enable the reader to bear in mind the different parts of this
division, which are persistent over a large extent of country, and seem worthy of being no-
ticed, as the mass is so variable in its different parts that it cannot well be described as one.
5. Thin-bedded dark grey or brownish limestone. Few cavities. Highly bituminous. Sometimes
contains nodules of hornstone. .
4. Thick-bedded dark or bluish grey limestone with irregular cavities, and often siliceous accretions,
or hornstone. Surface very ragged from weathering. Highly bituminous.
. A lighter colored subcrystalline mass, very irregularly stratified, contorted and concretionary.
. A bluish grey subcrystalline mass, mostly thin bedded, and separated by seams of dark shale.
. Grey or bluish grey siliceous limestone; hydraulic limestone, or beds of passage from the shale
.
below.
Few points west of Rochester offer so good an opportunity of examining all the parts of
this limestone in the order of succession. It is exposed and quarried at numerous places,
which will be noticed under the description of the rocks of Monroe county.
In the town of Ogden, the lower part of the limestone, or that following the hydraulic layers,
is charged with fossils, (principally Atrypa and fragments of the Trimerus.) The rock con-
taining them is extremely thin bedded, though a pure limestone. The upper part of the rock
in the same town is extensively developed, and appears in very heavy strata, abounding in
coralline fossils. -
88 GEOIOGY OF THE FOURTH DISTRICTs
In the next town westward, there is a light grey crinoidal limestone, which, from examina-
tions made elsewhere, is found to come in above the dark compact beds on the Genesee, and
below the concretionary mass (No. 3). It is abundant in loose fragments on the surface, but
cannot be seen in place except in one or two instances. It is wrought as a fire-stone, and,
from its porous nature, serves the purpose very well. It becomes more developed farther
west, forming the beautiful and durable crinoidal limestone of Lockport, and extending to the
Niagara river. s -
In the south part of the town of Sweden, the upper strata of the limestone contain an abun-
dance of coralline fossils, which, from the weathering of the surface, stand out in bold relief,
exhibiting their structure in a most perfect manner. The best specimens can be obtained
from the loose fragments, which are strewed over the surface in great profusion.
In its extension through Orleans county, this limestone forms two distinct terraces; the
more northerly one being produced by the lower part of the rock, and the southern one by the
higher strata. Its northern limit is from the town of Sweden to Clarendon centre; thence by
the south side of Jefferson lake, it continues west turning a little southward, and passes two
miles south of Albion and about the same distance south of Medina. The southern terrace,
or outcropping of the higher strata, is about two miles farther south.
In its lithological characters, this rock suffers little change throughout this county. Its
lower portions retain the character of a siliceous limestone, which continues, though somewhat
unequally developed, as far as the Niagara river. At Shelby falls, in the town of Barre, it is
unusually thick, and well exposed. From the former place the stone has been burned, and
proved a good hydraulic cement. The crinoidal portion of the mass, which is so extensively
quarried at Lockport, does not appear so well developed in Orleans county, though it exists
in all localities, having the same characters as in Monroe county. The quarries in this rock
afford an abundance of good building stone, and lime, and it is easily accessible throughout
the whole length of the county. In consequence, however, of this range passing from two to
four miles south of the canal, and all the large villages being along the line of the latter, there
has been little inducement to open extensive quarries, as stone is more readily supplied from
other points. -,
In Niagara county, this limestone passes through the towns of Royalton, Lockport, Cam-
bria and Lewiston, and extends into the next southern range of towns. Its greatly increased
thickness has rendered it an efficient protection to the shale beneath; and this, instead of
being worn down and spreading out over a broad surface, as in the eastern part of the district,
forms only the northern slope of this great escarpment, often presenting a width of less than
one quarter of a mile. This strongly marked feature of the country on the west of the Gene-
see is entirely lost on the east, from the thinning of the limestone. Nearly the whole width
of the formation in Niagara county is of the limestone ; while at the east, the shale covers the
greater extent of surface occupied by the group.
The two sections of Lockport and Niagara, the one an artificial and the other a natural one,
exhibit not only the limestone, but the whole group to the greatest possible advantage. At
Lockport the shale, as elsewhere, passes into beds of impure siliceous limestone; and these,
NIAGARA GROUP, 89
*
in their continuation upwards, are succeeded by a pure crinoidal limestone. So abrupt is this
change, that specimens can be selected, exhibiting both rocks in connection, as if one deposit
had succeeded the other instantaneously, allowing no lapse of time and no intermixture of the
tWO.
This is a continuation of the light grey crinoidal limestone which first appears in Monroe
county, but it has become much thicker and more compact. Near Lockport it is often varie-
gated with red, from the stems of crinoidea which are thus colored. These again lose their
color, and the mass is grey. At this place the rock is thick bedded, and in regular courses;
it is readily wrought from the quarry, and forms one of the best and most durable materials
for construction which the State affords. It has recently been extensively quarried for the
enlarged locks upon the Erie canal at this place.
The following is the character of the different beds, in the descending order, the lowest
resting on the impure hydraulic limestone. (The numbering is from the lowest upwards.)
5. Thinly laminated blackish grey limestone, with thin laminae of bituminous shaly matter; the whole
exhibiting a tendency to a concretionary or contorted structure, and the surface of the layers
marked by small knobs or elevations as represented in woodcut No. 29. --
4. Greyish brown bituminous limestone, the lower part with irregular cavities containing spar; this
passes upwards into more regular beds of a dark color, containing few cavities, but marked by
the presence of blende.
3. A dark colored limestone, with cavities and veins of spar, often concretionary.
2. Irregularly thick-bedded limestone of a light grey color, with numerous cavities containing spar, etc.
1. Encrinital limestone, often beautifully variegated with red; entirely composed of encrinital columns
and other fossils, which are always broken and worn. -
During the period of the deposition of this limestone, the condition of the ocean seems to
have been favorable to the production of corals, as is indicated by the immense number
crowded together in the central portions of the rock. Their partial or entire destruction as
before described, and their replacement by crystalline matter, renders them a less prominent
feature than they otherwise would be. Few shells appear to have lived after the deposition
of the lower strata; or if they existed, their forms have become obliterated. The broken and
worn fragments of corals and crinoidea indicate, during the earlier periods, a condition of shal- .
low water, as of a coral reef approaching the surface, where the force of the waves destroyed
all except some of the more solid forms. Subsequently the water seems to have deepened,
and the comminuted matter, produced by the action of the waves upon the higher portions of
the reef, settled down in the form of fine calcareous mud, enveloping the living corals at the
bottom. Toward the eastern extremity of the formation all these forms disappear, and the
limestone is composed of, what we may suppose to be, the finer mud derived from the de-
struction of the corals farther west. The condition, therefore, or the depth of water at the east,
prevented the growth of corallines; while in the west, all circumstances were favorable to
their production.
GEOL. 4TH DIST. - 12
90 GEOLOGY OF THE FOURTH DISTRICT.
The crinoidal mass forms the capping of the terrace every where in the vicinity of Lock-
port, and is the same in which all the quarries of importance are situated. It varies in texture
from fine grained, where the nature of the component parts can scarcely be detected, to that
where the stems are several inches in length. Where weathered, these stems stand out upon
the surface in strong relief, forming beautiful illustrative specimens for the cabinet. Plates
of the Caryocrinus ornatus, and fragments of corals, frequently occur together. The wood-
cut No. 26 is an illustration from a specimen found near the village.
º:WG º
2 sº
#3
§Yº
º
- E. W ... º -
w º ºw
Pºž º W º
º º
* - Kwº w
- *. -- º w
*- -- N
º- ºrs: º
§§
º É.
tº: sº
@) É º
ÉSºlºš º 22:32:3:...?
º #. à *::=::\S.
º ººs. Tº a º
22*...* º
Fragments of Encrimital columns in Limestone,
These stems lie in the greatest possible confusion, and many of them are much worn.
Perfect fossils are rarely found in this rock, all the materials having evidently been triturated
by the waves for a long period, while they formed a calcareous beach or bar rising to near
the surface of the ocean.
The succeeding mass contains a great abundance of corallines, some of them in the position
in which they grew; others turned upon their sides, or entirely reversed. Many of these are
in a very perfect condition; others are partially destroyed, and crystalline matter has taken
their place. The greater number apparently belong to a species of Porites of very delicate
Structure. -
In the third division the cavities are more abundant; and we often find, that surrounding the
edge of these, a portion of the fossil still remaining, marks its former extent. In other cases
a mass of coral is partially dissolved, with crystals of selenite penetrating it in every direction.
Again the coral is almost completely blended with the selenite, as if it had been rendered
NIAGARA GROUP. 91
nearly fluid before the change took place. Masses of the coral often present cavities, from
which crystals have been dissolved, leaving the spaces with their sides as plane and smooth as
if cut with some sharp instrument. These examples show how limited may be the influence
producing such changes. No effect appears to have been produced in the least beyond the
edge of the crystal, or the space it once filled; but by what means solution could take place
in right lines, it is difficult to explain. The coral in many such cases has scarcely suffered
any change from its living state, presenting the same porous structure as recent specimens.
27.
The illustration represents a specimen of Porites with linear cavities, from which crystals
of selenite or some other mineral have been dissolved. The cavities here shown are their
actual size; in this instance being small, but in others they are several inches long; and I have
seen a large hemispheric mass of coral completely divided by a plate of selenite, half an inch
thick, its limits perfectly defined. Some portions of this selenite still retained the markings
of the coral, which apparently was not entirely converted to the sulphate.
An appearance very similar to this occurs in the Water-lime group, and also in the shaly
limestone of the Onondaga-salt group. Numerous linear cavities present themselves upon the
surface, generally offering no evidence of having been filled; but in some instances, where
there has been no exposure, and moisture has had no access, they are still filled with crystals
of sulphate of baryta. Specimens have been obtained where the exposed edges were covered
with cavities, while the fresh surface presented innumerable acicular crystals imbedded in the
rock. In these cases, we may suppose the crystals to have been segregated during the so-
lidification of the mass. But we cannot account in the same way for the cavities in the coral,
92 GEOLOGY OF THE FOURTH DISTRICT.
nor for the presence of crystals; for these could only have taken place after the growth and
formation of the solid structure. -
Both in this and the next succeeding division of the rock, spheroidal cavities are scattered
in great profusion, and without order. Certain layers, however, yield the finest specimens of
dogtooth spar, and others of pearl and brown spar; while the selenite and sulphate of stron-
tian are confined to one or two strata, and are rarely found elsewhere. These facts are of
interest, and future investigations will probably reach the true cause, whether it may have
been in certain genera or species of corals, or from other sources that the sulphates resulted.
The anhydrous gypsum which occurs in this rock, fills cavities in a mass lower than the sele-
nite and sulphate of strontian, and principally below the spar, though often occurring with the
latter. -
Besides the tendency to spheroidal or concentric concretions, there is sometimes a tendency
to a thickening of the strata, probably due to the same influences, and which often produces
apparent undulations in the succeeding ones. An example of this kind is given in the following
woodcut. It appears in the bank of the canal two miles south of Lockport. The elevation
is entirely produced by the thickening of the mass, the strata being horizontal below. The
succeeding strata are seen to thin out as they approach this thicker portion.
28.
É
==== ɺ ºw
2: ####: w
º
º -- # - AºE -
EEEsº
- Eº-º-º-º-º:E--->
tº- º:---->s-ºs->:-
==*
sº-º-º-º-º-º-º:
:-->
Farther south the higher strata seen in this illustration disappear, and a mile beyond this
point some still higher rise above the level of the canal; these constitute the terminal portion
of the rock. They are thinly laminated, from the intervention of a black bituminous shaly
matter. The layers are all curved, the extremities bending downward. The surfaces are
again covered with little knobs or incipient concretions, the convex upper surface of each
having a corresponding concavity on the under side; presenting an appearance as if impressed
with the fingers while in a yielding condition. These appear like what may sometimes be
seen in a semi-fluid viscid mass when heated, or from which gas is evolved, raising the sur-
face into a great number of small bubbles. Those upon the stone, however, are infinitely more
NIAGARA GROUP. - .* 93
numerous and regular than any thing of this kind. The following woodcut is an illustration,
reduced one half, from a specimen from this locality —
|
º
º
St.
ºš
$
“...sº
sº
º Š
:=
º-º-º-º: =sº *.
=ºğsº §§§
ësº §§§ §§§
§:
Concretionary structure in the strata south of Lockport,
It will be observed that these elevations are not all circular, but often confluent, forming
little rounded ridges, sometimes several inches long, and again interrupted. The knobs in
like manner are often arranged in lines, and they not unfrequentl
quincunx order. •'
I have seen an instance in the same rock where several knobs became enlarged and much
elevated, breaking through the superincumbent laminae; and the surface of the shaly matter
at the junction presented the smooth and striated appearance common,
moves over another, as in the sides of faults in strata.
At Porter's quarry, one mile east of Niagara Falls, the Structure, though somewhat different
from that of the same strata at Lockport, exhibits the influence of similar causes. The whole
is thin bedded, and arranged in curved or dome-shaped layers, the ends bending downward,
and continuing for many rods with the same regularity as in the figure. In some instances,
for a short distance, the layers are much more abruptly curved than in this illustration.
y present themselves in
where one hard surface
94
GEOLOGY OF THE FOURTH DISTRICT,
The woodcut represents the strata as they appeared, looking in the direction south by east,
and against the edges of the layers, which are crossed by vertical joints, having a direction east
by north and west by south. The extent of each curve is from one to two feet; sometimes a
single one divides and forms two. There is here no evidence of a breaking up of the strata
below, and consequently there has been no uplifting process to produce these curvatures.
appears rather due to the accretionary force, which induced a tendency to curving or folding
in the laminae throughout the mass, operating with great uniformity and over a wide extent.
These curves seem due to like causes with those small ones at Lockport, which are usually
Sºº-ºº: R.
#######
|
ſ
º § #33 º § 6 º: 㺠# [.
#išū;ºſſjīlī; išiū!!!
Fº
ºi | |||}|†† jºiſſiºiº
º |Wijī jī! |ft|#| ||
ºfflº
*i; }; ºffſ ††† *
iſſ iſſi; th
iſſºjip jājp
Hºllipſºs:
š:######2-#:##########
º:==:
--~~s -:
lºlºſ | İğiſſiº
º ##jº |||
>: #ſº §: ######3 š 3:3: &
º
º
**..
Curved strata—Porter's quarry, Niagara Falls.
less than one inch in diameter.
There seems no reason to doubt that all these appearances are due to the same action which
produces well-defined concretionary forms in other situations, and under more favorable cir-
cumstances. The oolitic and concretionary character of this formation in some parts of the
Third District, seem to be represented in a great degree by what is here exhibited in the
terminal strata.
The same structure exhibited in the two last illustrations occurs in the Third District, as
illustrated by the following woodcut from Mr. Vanuxem's Report:
31.
ºss
2. º > -º
%. § sºs
ºššš º
===sºsºs:
> .
NIAGARA GROUP, . 95
The drawing fig. 1, is from a specimen, and of the natural size. The curving of the laminae
is precisely as in the quarry at Niagara Falls, and intermediate between that and those of
Lockport, where they are much smaller than in this figure. In a few instances at Rochester,
some thin strata exhibit the appearance represented in figure 2, where the rock, after being
partially hardened, was broken up, and again cemented. The cementing matter is usually
crystalline. These appearances are more common in the central portions of the rock, and
are not seen in the higher strata. - -
The lower and middle portions of this limestone, in addition to the regular seams or divi-
sional planes, often present a kind of undulating seam or suture, the projecting portions of one
layer closing into corresponding depressions in the other. These, from being scarcely visible,
become of considerable magnitude, and the projecting portions on either side an inch or more,
and even five or six inches in length. These have been compared by Mr. Vanuxem" to the
sutures of the skull, which they often resemble. When separated, the surfaces present a
parallel fibrous or striated appearance, and are frequently covered with a film of carbonaceous
matter. These appearances, which occur not only in this rock, but in the water lime and
some of the higher rocks, were termed by Prof. Eaton, Lignilites, from their resemblance to
woody fibre. They are not always at the junction of two layers, or as forming a division,
but frequently penetrate the solid stratum, and are separable, appearing like a wooden pin
driven into the mass. Again they divide the rock into columnar blocks of variable dimensions.
The illustration No. 32, is from a specimen where the striated surface is eight inches long,
and has separated a portion of the rock into an irregular column.
->3:s:s: - d t
*E:E:s: 3 ºr g iſit
* = ºs-ºs- tº- ºss-º-º: ºf . .
jº º:Sā;. |: | | || ||
* 3ºEºs::ſiliº
| ºl; lºsº: |
º: #| || || || ||
§
\ | |
º
º: º -
: =######## -º
--- º::: º
Eºs: £5:EE::=º ºr º-> E”
º É §ºs::==35:
Es--> & :::::: º ºg *=º
=#E=#3:35.
###33-#3 #ſº Wº
ºf W \ ë º
§§ | w
º \|| ||
Vºlºſſ l
} § \\ d | | - | l
| º | || É - !
º
{{ º \ Ä º -
W. "Wºº º º ſ
§§ º Will {||||||}||
\ºſſ'ſ #|| | || || | |
| \\\{{{ | |
|||||||| |||} ſ º
||||||}|
º º N
º º!"
|\ º | s |
º §% º|| ||
|\% º|| |||||}|| || ||
* Annual Report of the Third District, for 1838, p. 271.
96 GEOLOGY OF THE FOURTH DISTRICT,
Mr. Wanuxem suggests that this structure is due to the crystallization of sulphate of mag-
nesia in the fibrous form, which penetrated the rock, and produced the striated surfaces; that
it has since been dissolved, and that probably the same water which dissolved the saline matter
deposited the carbon which invests the surfaces. We find in many instances where this struc-
ture occurs, that the interstices are still occupied by carbonate of lime in long fibrous crystals;
and it is suggested whether this mineral, as well as some others, may not have been the cause
of their production. These appearances are very obvious in many places where there has
been a fresh exposure, and weathering removes the carbonaceous matter.”
Topographical features. – In the eastern part of the district the limestone is thin, offering
little protection to the shale, which is consequently worn down to a very gentle inclination,
presenting a much greater breadth of surface than farther west. The limestone, becoming
thicker in the same direction, occupies a broader space, while the shale is seen only in its
outcrop. The nature of the two masses has given origin to much interesting scenery along
its northern margin; every stream crossing it has its rapids or cascades. The fall and deep
gorge at Wolcott village is the first of importance within the district. Several points of minor
interest occur between this and the Genesee river; but from the great accumulation of drift,
and the absence of large streams, the rocks are not well exposed. On the Genesee, the group
gives origin to the upper fall at Rochester, the rapids above, and the cliffs below, which to-
gether display both divisions in great perfection. The falls at Shelby, three miles south of
Medina, on the Oak-orchard creek, are over the lower limestone and shale of this group. The
“mountain ridge,” before alluded to, continues a distinctive feature of the scenery from the
Genesee to the Niagara river; and the numerous deep and picturesque gorges in the margin
of this cliff sufficiently indicate the former existence of streams of great magnitude, or an
excavating power operating from the north. - - -
Finally, this group gives rise to the grand Falls of Niagara, the wonder of the world, and
a geological monument by which to measure its periods, and enable man to compare the past,
the present and the future, and thence deduce the formula for determining the duration of
those eras in years, which are now only known by the exhibition of phenomena which cannot
indicate dates, or computation of time in human periods. .
Localities. – The principal localities have been enumerated in the description of the group;
a few of these will give the observer an acquaintance with the variations in character which
the rock assumes in its western extension. The most eastern localities are in the towns of
Wolcott and Butler, the former exhibiting the shale and the latter the limestone. In order to
observe the gradual changes which the limestone undergoes before its full development at
Lockport and Niagara Falls, a few other localities in Wayne county should be examined, as
the quarries in the towns of Williamson and Marion. Along the Genesee at Rochester we
find one of the best exposures in the whole district, and this is a very desirable point for in-
* See also the same structure represented under the Onondaga-salt group.
NIAGARA GROUP. 97
vestigation. At this place, its characters are intermediate between those in Wayne county
and Niagara. In the towns of Ogden and Sweden, the limestone presents some interesting
features not observed at Rochester. In the towns of Clarendon and Barre, and at Shelby
falls, as well as at many other localities in Orleans county, there are good opportunities for
investigating the rocks of this group.
The vicinity of Lockport will give the geologist, or the student, all desirable information
regarding this interesting group of rocks; but he must still visit Niagara, to see them in the
locality which will be remembered and known for many thousands of years. The rocks of
the Niagara group are exhibited along the whole of the immense gorge or chasm of seven
miles below the Falls; at first near Lewiston forming about one hundred feet of the upper
part, and at the Falls being all that is visible above the river below.
The section of the Niagara river from Lewiston to the Falls (Plate 3), is a transcript of the
eastern bank as seen from the Canada shore, and exhibits the order of arrangement among
the strata in a perfect manner. At the brow of the terrace above Lewiston, the shale of this
group is seen to succeed the Clinton group, and is capped with a few feet of limestone.
Thence it dips gradually southward, the limestone increasing in thickness all the distance to
the Falls, where the shale, from being two hundred feet above the water as at Lewiston, has
approached to within a few feet of it. The river descends in this distance about one hundred
feet; and the level is continued in the section from Lewiston, showing this depth of water
below the Falls. -
The same order of succession is exhibited at Niagara Falls as at Lockport; and by de-
scending the staircase to the ferry, or at Goat island, the character of the strata may be seen
as far as the shale. The upper part of the limestone, however, is not there visible, the highest
seen being the dark brown mass below the upper one. The terminal portion of the rock is
seen nearly a mile east, at Porter's quarry. .
Thickness. – The thickness of the shale of this group suffers little variation throughout the
district. At Wolcott, its thickness, by estimation, is little less than one hundred feet; at
Rochester, it is of about the same thickness; at Lockport, it is eighty-one feet by actual
measurement; and at Niagara Falls, and along the river, it preserves the same, not varying
more than one or two feet. The limestone is apparently not more than thirty or forty feet
thick in Wayne county, but gradually increases westward, being about seventy or eighty feet
at Rochester, and one hundred and sixty-four feet at Niagara Falls. This thickness at Nia-
gara is obtained by measuring the perpendicular bank at the Falls, and levelling from thence
to Porter's quarry, nearly a mile east of this point, where the higher strata are seen.
[GEOL. 4th DIST.] - 13
98 GEOLOGY OF THE FOURTH DISTRICT,
Mineral Contents of the Group.
In this group, we find a greater amount and variety of crystallized minerals than in all the
other rocks of the Fourth District. The absence of disturbance, or the influence of hypogene
or metamorphic masses, leaves the rocks of this district comparatively barren of simple mine-
rals, which, under favorable circumstances, would have been largely segregated, as we find
them in some of the lower strata, when in the proximity of crystalline rocks.
From the decomposition of the shale, results sulphate of magnesia, sulphate of alumina,
and muriate of soda or common salt, which are found in sheltered situations along the banks
of the Genesee and Niagara rivers. Sulphate of alumina, in beautiful efflorescent forms, is
produced from the upper part of the shale during the process of calcination. Nodules of
gypsum, usually replacing some organic body, are of frequent occurrence. The superior
extremity of the Caryocrinus ornatus is frequently filled with snowy gypsum, sometimes the
plates remaining, but a little separated; at other times, they have entirely disappeared. More
rarely, cavities are found lined with dogtooth spar. In the upper part of the shale, and lower
part of the limestone, green carbonate of copper is frequently found. Iron pyrites is univer-
sally diffused through the shale, and hastens its decomposition.
It is in the limestone, however, that we are to look for the minerals so characteristic of the
group. The abundant cavities or geodes, resulting in part, if not entirely from the decomposi-
tion of fossil bodies, are always lined or filled with some crystallized mineral. The most
abundant are dogtooth spar, pearl spar, brown spar, selenite, sulphate of strontian or celestine,
anhydrite, and more rarely fluor spar, crystallized zinc blende and galena. These minerals
are variously grouped and associated; the more common forms, however, are found in all
situations in the rock, while others are confined to a single stratum or two.
The calcareous or dogtooth spar is usually of a yellowish color, and in small crystals. The
fluor spar is in small cubic crystals of a delicate straw color. The blende is often associated
with pearl spar, some portions of the rock having all the cavities lined with the latter mineral,
to the almost entire exclusion of the dogtooth spar. The latter is more abundant in the darker
colored limestone, overlying the light grey which abounds in pearl spar, and is frequently
associated with the latter of a delicate pink color. t
The celestine often occurs in beautiful groups of crystals, penetrating masses of selenite.
Fine specimens of the latter are frequently obtained where the spars are enclosed in the
transparent mass.
Zinc blende is more common in the higher dark-colored portions of the limestone, and above
the point where the greater quantity of spar and other minerals occur. It is that part of the
rock which forms the margin of the cliff at Niagara Falls; and here as well as at Lockport,
this mineral is common, though the quantity is not great. Galena often occurs associated
with the blende, and sometimes in a lower situation ; it is seen in small masses, but more
generally in threads or thin veins, often apparently as if filling fissures. I have obtained spe-
cimens of this kind at Rochester, where, on fracture, the two sides of the stone presented a
NIAGARA GROUP. - 99.
thin film of the ore. In excavating the limestone near the Whirlpool, specimens were obtained
which were crossed by numerous thin veins, sometimes one-eighth of an inch thick. I was
also informed, that during the excavation of the Erie canal at Rochester, several hundred
pounds of galena were found in a single cavity. This is perhaps not improbable, and the
celestine and gypsum sometimes occur in masses of nearly equal weight. -
In some of the geodes, and among the crystals of calcareous spar, there occur long pris-
matic crystals of a dark brown color, which appear like black hairs; they are attached to, or
penetrating the calcareous crystals. This mineral has usually been referred to Rutile, but
Dr. Beck regards it as Achmite. ! . . . -
Iron pyrites occurs in the limestone, as well as in the shale; but in the former, it is usually
in nodules or irregular masses.
Native sulphur is of common occurrence in the small cavities in the encrinital limestone at
the Cold-spring quarries, two miles east of Lockport. * . . h
Calcareous tufa is formed in many situations, where water, percolating through the lime-
stone, finds an outlet in the shale. The deposition forms in the fissures of the rock, and finally
accumulates in large masses projecting from the sloping edges, until from its increased weight
it falls down. Instances of this kind may be seen in the banks of the Genesee below Ro-
chester, and in similar situations at Lockport and elsewhere.
Springs charged with sulphuretted hydrogen occur both in the shale and in the limestone,
though not usually very copious. The localities of some of these will be enumerated under
the respective counties in which they occur.
Springs.--From the nature of the two rocks forming the group, the line of junction every
where gives origin to springs, which flow over and fertilize the northern slope of the escarp-
ment. The limestone, from the numerous vertical joints, is pervious to water; and toward
its northern limit, the soil is often dried in consequence. The shale, from being impervious,
holds up the water thus falling upon it, and from the southern dip, operates as a reservoir,
affording a constant supply in the springs which break out along its northern edge. This
character is more obvious in the western counties; while farther east, from the more gradual
slope of the shale and thinning of the limestone, the springs rarely appear on the surface, but
the water is disseminated through the soil.
Agricultural characters. — The two members of this group are marked, to a considerable
degree, by a difference in the soil. The destruction of the shale has given rise to a clay,
which, mingling with the more sandy production of the Medina sandstone on the north, has
produced a soil of unequalled fertility ; and there is rarely, if ever, to be found a better wheat-
growing soil than the portion overlying this rock. In some places it has a greater amount of
argillaceous matter than is desirable, and forms a stiff soil; but where the slope of the surface
is sufficient for effectual drainage, it produces no inconvenience.
The soil covering the limestone, particularly where it is a little elevated above the country
on the north, is of a loamy character, the argillaceous nature of the mass below having had
13% .
4. o
º
tº sº g
* e ſe
*
*
100 GEOLOGY OF THE FOURTH DISTRICT.
little influence. In many places, however, for a small extent, the surface is clayey, and even
extremely so, as if the materials of the lower rock had been deposited upon the higher. An
example of this kind occurs a little west of the village of Lockport, where the limestone is
covered by a clayey soil, while, a mile or two further east, the soil is a light loam. The
latter character also prevails in some places near Rochester, and at other points along the out-
crop of this limestone. This character of the soil, together with the rapid drainage to which
it is subjected, from the fissures or joints in the limestone, as well as the proximity of the rock
to the surface, has given rise to a different growth of timber, which everywhere marks the
limestone terrace. While the country on the north and south sustains a forest of maple,
beech, elm, ash, and the associated forest trees; that along this limestone is indicated by oak,
chesnut, and others of the same nature. -
Following the slope of the limestone southward, the soil becomes more clayey, and the
surface more level. - - -
Organic Remains of the Niagara Group.
One of the most striking features of this group, and particularly of the shale, is its vast
number of organic remains. Shells and trilobites are the most abundant forms, though several
species of Crinoidea are common. Corals of different genera and species are the predomi-
nating forms in the limestone, while shells and trilobites are rare. In this group in the Third
District, organic forms are rare, few species only being known ; while they become more
abundant in Wayne county, constantly increasing in a westerly direction as far as Lockport.
Along the Niagara river the means of examination are limited, notwithstanding the fine natural
section; but in all accessible localities, the same fossils are found as elsewhere. *
We have, in the shale of this group, no less than six species of Trilobites and nine species
of Crinoidea, with as many shells, which occur in no other group within the district, and have
not been seen in any other rock elsewhere in the State. -
The partial or entire decomposition of the corals in the limestone has, in a great measure,
prevented their affording the characteristic distinctions they otherwise might have done.
TRILOBITES.
Among the Trilobites, the following are known as characterizing the shale at Rochester,
Lockport and other places. Two other species are known in this group, which will be found
figured in a lithographic plate at the end of the volume, and there is still a third form which
has not been described.
NIAGARA GROUP. {{}}|
2 #:
4 :
3 s
º ɺ
àº
1. Asaphus limulurus. 3. Calymene Niagarensis.
2. Head of Asaphus limulurus. 4. Bumastis Barriensis.
1. Asaphus limulurus (GREEN, Monograph, p. 48.) – This fossil is known by the great
length of the caudal extremity, which is often produced nearly an inch beyond the articula-
tions. The form figured is the most common, and will be recognized as the most abundant
of the Trilobites at Lockport.
This species is remarkably similar in many particulars to the A. longicaudatus of Murchi-
son, but differs from it in the shorter tail and the greater width at its base, being much less
slender. It has also fewer articulations in the post abdomen, ten or eleven being the extreme
number. With these exceptions, our fossil is very similar to the English one, and apparently
holds the same place in the series, eminently characterizing the lower part of the Niagara
group as that does of the Wenlock; these formations of the two countries being equivalent,
so far as we are able to decide. t
2. Head of Asaphus limulurus. – The head of this species being so abundant at Rochester
and other places in Monroe county, where perfect specimens are rare in the ordinary expo.
sures of the rock, that it seemed desirable to present it as it there occurs. The eyes are
usually detached, their form only being perceptible. The anterior portion of the buckler is
produced in a blunt point, its posterior angles extending backward and terminating in acute
points, which, in perfect specimens, reach to the fifth rib of the abdomen. Each side of the
middle lobe of the head is marked by three indentations or furrows, the anterior one extending
obliquely forward.
102 GEOLOGY OF THE FOURTH DISTRICT.
3. Calymene Niagarensis.-The middle lobe of the head of this trilobite is marked by
three rounded protuberances on each side; the front one very obscure, and sometimes scarce-
ly distinguishable; the posterior one very prominent. Eyes small, not reticulated, opposite
the central protuberance of the middle lobe. It has thirteen articulations on the back, and
eight in the tail. The surface is entirely covered with minute rounded tubercles.
This fossil has usually been referred to C. Blumenbachii, as well as to the species in the
Trenton limestone; but our fossil differs from the last, in the more rounded posterior angles
of the buckler, and in other particulars; from the former it differs in being uniformly of the
small size represented, in having but thirteen articulations in the back, and in the less pro-
minence of the protuberances on the middle lobe of the head. It seems extremely doubtful
whether all the figures given in the works of foreign authors under the name C. Blumenbachii,
are of that species. A form referable to C. Blumenbachii (Silurian Researches, pl. 7, fig. 6),
occurs in the Schoharie grit, and several fine specimens have been obtained by Mr. Gebhard
of Schoharie. By reference to the table of strata, it will be seen that the fossil described
holds a much lower position. -
Locality—Lockport, in Niagara shale; also at Rochester and intermediate points.
4. Bumastis Barriensis (MURCHISON, Silurian Researches, p. 656, pl. 7 bis, fig. 3, a, b,
c and d, pl. 14, fig. 7, a and b). “Head round in front; margin raised; oculine protuberances
large, surrounded by a depression, on the edge of which, over the eyes, [are] two small ovate
prominences; in advance of the eye, and towards the margin, two slight hollows. Eye ap-
proaching to semilunar, apparently smooth. The facial suture traverses the oculine pro-
tuberances, separates the upper portion of them from the eye, and passes under the margin.
Body with no true longitudinal furrows; central lobe only just perceptible by a slight depres-
sion in the body only. Ribs 10, those of the lateral lobes terminating in recurved blunt ends.
Caudal portion round and smooth, without a trace of trilobation. Surface of the whole animal
covered by extremely thin, apparently imbricated lamella, the edges waved or vermiform, the
intermediate spaces studded with minute dots.” -
This trilobite is readily recognized by the similarity of the two extremities, which are much
more rounded than in Isotelus. It is known at the locality as the “Double-headed Trilobite.”
Our specimens are usually much flattened, and the oculiform protuberances scarcely elevated.
Although there is no distinct trilobation of the body, there is usually a strong undulation in
the ribs at the point between the central and lateral lobes. After the removal of the crusta-
ceous covering, the body is sometimes seen to be covered with minute punctae. In our spe-
cimens, the length of the body is from one third to two thirds the length of the caudal extre-
mity: this circumstance, with the apparently more slender ribs, at first induced me to consider
it a distinct species.
Locality—Lockport, in Niagara shale. The head and caudal portions of this fossil are
often found at Rochester, and in Wayne county, but I have seen no perfect specimens from
these localities. -
NIAGARA GROUP. 103
- º |
§ '
# º ;
|
# NSºlº: º
§ º
| #. ſºlº | | } }
º º º
Fº
º
iš §
º
ſ:
º :
;
t
|
*
-º# ,
|
|
|
i
ſ
|
Homalonotus delphinocephalus.
Homalonotus delphinocephalus. (Silurian Researches, pl. 7 bis, f. 1 a, 1 b. Trimerus
delphinocephalus, GREEN, Monograph, fig. 1, p. 82.) — Head depressed, ovate, sub-acute,
or rounded anteriorly; eyes prominent, rather small. Body composed of 13 ribs, with inter-
costal plates; extremities of the ribs directed forward. Caudal extremity distinct, with 12
ribs united, forming a solid crust; tail acuminate. The whole surface is papillose, or sca-
brous, and in the least exposed portions, this character is often preserved in great perfection.
It is among the most common trilobites at Lockport. The specimen figured is two-thirds
the natural size, and they have been seen of twelve inches in length. The young of this
species, figured by Green, is often found, and sometimes less than an inch in length. The
name Homalonotus of König has precedence over that of Trimerus, but the specific name of
Green has been retained by Mr. Murchison. -
This fossil and the Dipleura Dekayi have often been most unaccountably confounded with
each other, notwithstanding their geological relations are so widely different. Dr. Green has
quoted Lockport as a locality, where he remarks it is not uncommon. Rochester, in the same
geological position, is also named as a locality. All the other places named as producing the
Dipleura, are in the higher rocks of the system. The separated heads of these species very
closely resemble each other, but the nature of the matrix is usually very different; and during
all the excavations at Lockport, I have seen nothing referable to the Dipleura. -
Localities—Lockport, Rochester, Sweden, Wolcott, and numerous intermediate points.
104 GEOLOGY OF THE FOURTH DISTRICT.
SHELLS.
Strophomena (Leptana), and Delthyris (Spirifer), are the most abundant forms usually
seen. One or two species of Atrypa and Orthis are scarcely less numerous.
The following are the more common forms of Strophomena:
35.
# A
º \,\ ,
| º, º
º NA’
WWYY
|\ \\\\\ sº
º - º
5 **
（ſºlº
1. Strophomena subplana. 3. Strophomena striata.
2. S. depressa (lower valve). 4. S. transversalis.
1. Strophomena subplana (ConRAD, Jour. Acad. Nat. Sci. Vol. 8, p. 258). This shell
is distinguished by the sharp radii which alternate in size, and by the nearly flat valves. It
often occurs in beautifully preserved specimens upon the surface of thin calcareous layers
in the shale. When imbedded in shale, the radii are not so prominent. It is the largest
species of this form in the group, but is often smaller than the figure.
Locality—Lockport, Niagara, Rochester and Wolcott.
2. Strophomena depressa. (Productus depressus, M. C. t. 459. Leptana depressa, DALM.
Swedish Transactions, p. 106, t. 1, f. 2; His. Pet. Suec., p. 69, t. xx, f. 3. MURCHIsoN,
Silurian Researches, p. 623, pl. 12, f. 2.)—This shellis abruptly deflected in front; the slight-
ly convex or flat surface marked by six to eight folds or undulations, which are crossed by nu-
merous striae. The sides of the shell at the extremities of the hinge are expanded into wings.
This portion of the fossil is usually obscured by the matrix, which when removed displays
the form as figured.
The deflected portion of the shell is not as long, and the undulations not as numerous as in
the figure of Mr. Murchison. Specimens from the same rock however, apparently of different
ages differ in these particulars. The fossil commences its existence in the Clinton Group,
becomes very abundant in the shale of the Niagara Group, and continues through several of
the higher formations. It occurs in every locality of the Niagara shale, though usually smaller
than the one figured, and often apparently more circular. -
3. Strophomena striata, shell semi-elliptical, lower valve slightly convex, upper one flat,
finely and equally striated, the striae dividing; a few punctulations appear near the margin of
the shell, which were probably furnished with minute spines. The valves are usually sepa-
rated and spread over the shaly laminae. Its delicate striated surface distinguishes it from
others of the group. Locality—Lockport; Rochester. - -
NIAGARA GROUP. 105
4. Strophomena transversalis. (Leptana transversalis, DALM. l. c. p. 109, t. 1, f. 4 ;
His. Pet. Suec. p. 69. t. xx, f. 5. MURCHIson, Silurian Researches, p. 629. pl. 13, f. 2.)—
Semi-circular, lower valve very convex, upper one very concave, finely striated, and marked
with linear distant, elevated ribs; “hinge inflected; hinge line straight, equal in width to
the width of the shell.” Our specimens are smaller than the figure of Murchison, and less
prominently ribbed. Locality—Rochester; Wayne county, and more rarely at Lockport.
36.
f
º
à
à
º
§
º 8
|
ſ
% % % g |
%/||
& / |
(ſ) §!
º
ſº
tº
§ ſº/º Š:
# |W §
&º
º
# º §
% § §
Jº
º
1. Delthyris Niagarensis, 4 and 4 a. Delthyris decemplicata. 7. a. º. o. Orihis hybrida.
2 and 2 b. D. radiatus. 5. Orthis Flabelluluna (a) ' 8. Delthyris sinuatus.
3 and 3 b. D. staminea. 6 Orthis canalis.
1. Delthyris Niagarensis. (CoNRAD Jour. Acad. Nat. Sci. p. 261.) – Semi-oval; ven-
tricose in the middle, (but generally flattened from compression); ribs about twenty-two,
rounded, not usually more than ten distinct on each side of the mesial fold, which on the
upper valve is prominent, rounded, and expanding towards the base; whole shell covered
with fine radiating striae, and usually a more prominent line in each depression between the
ribs, the mark of which is sometimes left in the cast; hinge line shorter than the greatest
width of the shell, rounded at the extremities. Width of the shell, one and a half inches;
length about one inch, but variable from compression. " ..
This fossil is peculiarly typical of the group, and will be readily recognized by its rounded
ribs and finely striated surface, differing from all others of the genus in this part of the
system. -
Locality—Lockport, Niagara, Rochester, and less abundantly in Wayne county.
GEOL. 4th DIST. 14
106 GEOLOGY OF THE FOURTH DISTRICT,
2 and 2 b, Delthyris radiata. (Spirifer radiatus, M. C. t. 493. Silurian Researches,
p. 624, pl. 13, f. 6.) — Semi-oval, ventricose, (often flattened from compression); shell
covered with fine radiating striae, scarcely interrupted by lines of growth; extremities of the
hinge line rounded; area moderate; perforation small. *.
Fig. 2 is from the shale and somewhat flattened; 2 b, is from the succeeding limestone and
is more ventricose, not having been compressed. -
This shell, in its various phases, resembles too closely the figures, both in the Mineral
Conchology and the Silurian Researches to be referred to any other species. The descrip-
tion in the latter corresponds with our largest specimens. It ranges from the iron ore beds
of the Clinton group to the Niagara limestone, but is more abundant in the shale of the latter
group. ; -
Locality—Wolcott, Rochester, Lockport, and numerous other points.
3 and 3 b. Delthyris staminea, n. s. (References. Spirifer crispus 2 Silurian System, p.
624, pl. 13, f. 8. Delthyris crispa, DALM. l.c. p. 122, t. iii, f. 6; His. Pet. Suec., p. 73, t.
xxi, f. 5.)—Semi-circular, lower valve very gibbous, and produced into an incurved beak,
upper one moderately elevated in the centre; ribs, commonly two in the upper, and three in
the lower valve on each side the mesial fold, crossed by numerous elevated, thread-like lines;
beaks remote, extremities of the hinge line rounded; area large. Cast of shell smooth.
This shell resembles the figure of Spirifer crispus 2 (Silurian Researches.) Hisinger's
figure differs from Murchison's and is less like our shell. I have obtained casts of a shell
very similar, if not identical with this one, from the “coralline limestone,” below the water-
lime at Schoharie. -
Locality—Common in the lower part of the shale at Lockport and Lewiston, less abundant
at Rochester and Wolcott. -
4 and 4 a. Delthyris decemplicata, n. S. Sub-triangular, gibbous, ribs ten, finely striated
longitudinally, and crossed by undulating imbricated lamellae, which are less prominent on the
mesial fold; mesial fold of the lower valve deeply impressed toward the margin and elevated
in front. tº
This shell is distinguished from the last by the greater number of ribs, which are crossed
by imbricated lamellae, while in D. staminea, these are simple elevated lines. From com-
pression these two shells often approach each other in form. There are usually four ribs in
the upper, and five in the lower valve, on each side the mesial fold. It much resembles
Spirifer octoplicatus, M. C. t. 562, f. 2 and 3; but the surface is striated, the mesial fold is
not plain, but the lamellae are less prominent than on the ribs. -
Locality—Lockport and Lewiston, occurring with the last named species, and more abun-
dantly. -
8. Delthyris sinuatus. (Terebratula sinuata, Sowerby in Linn. Trans. Vol. xii. p. 516,
t. 28, f. 5 and 6; Delthyris cardiospermiformis, His. Antechn. Vol. iv. t. 7, f. 6. DALM. sur
les Terebratules, p. 124, t. 3, f. 7; His. Pet. Suec. p. 74, t. 21, f. 9. Spirifer cardiosper-
NIAGARA GROUP. - 107
miformis, Von BUCH, sur les Spirifers et Orthis, t. 1, f. 7. Silurian Researches, p. 630, pl.
13, f. 10.) Obcordate, deeply two-lobed, striated longitudinally; lower valve convex, with
an incurved beak, upper one flat or slightly concave; area triangular, large in proportion to
the size of the shell. &
Our specimen is smaller than the one figured by Murchison, but it agrees so closely with
his figure and description, as well as with the figures of Von Buch and Hisinger that there
remains no doubt of its identity. This shell resembles the D. varica, CoNRAD, Jour. Acad.
Nat. Sci. Vol. viii. p. 262, pl. 14, f. 20; but in that shell the valves are nearly equally con-
vex, and the hinge line less extended. .
Locality—Wolcott, Sweden, Monroe county.
5. Orthis flabellulum (a)? (Silurian Researches, pl. 21, f. 8. O. callactis? DALMAN). —
Semi-oval, with 24 to 28 simple, rounded, smooth radii, which are crossed by a few lines of
growth; the radii continue strongly marked quite to the beak, their breadth being equal to
the spaces between them ; hinge line slightly arched, a little less than the width of the shell;
upper valve flat, the lower one slightly convex. Length 8 lines, width one inch.
In Murchison's figure the ribs are broader than in our shell; the description corresponds
with the exception that there are oftener 26 than 24 radii. I have seen a shell which is ap-
parently identical with this one, from the limestone of the Clinton group, associated with
Pentamerus oblongus. It differs from a similar shell in the Trenton limestone in the greater
number of radii, and the less convexity of the lower valve. The radii in the latter are often
bifurcate, while they are never so in the former.
Locality—Lockport; Rochester.
6. Orthis canalis (Silurian Researches, p. 630, pl. 13, f. 12, a.; also pl. 20, f. 8. Orthis
elegantula? DALMAN. Von BUCH sur les Spirifers et Orthis, pl. ii, f. 3, 4 and 5).-Semi-oval,
finely radiated, radii dividing towards the margin; lower valve very convex, with a produced
incurved beak; upper valve nearly flat or with a slight depression along the centre, which is
rarely characteristic in our specimens; hinge line shorter than the width of the shell.
This shell is every where found in the shale of the Niagara group, and is one of its most
characteristic fossils. It is somewhat variable in form, being often nearly circular; and is
evidently identical with the figure of Murchison, and is probably the same shell figured by
Dalman. Von Buck remarks in his description of this shell, that, it is found of precisely the
same form as the Swedish specimens, but a little smaller; at Castle Hill, Dudley, and at
Wenlock Edge, Shropshire. . . .
In the Delthyris shaly limestone of the New-York system, there is a shell almost precisely
similar in form to this one, but more robust ; the lower valve is very convex, almost carinated
in the centre, the upper one slightly convex, and marked with a depression along the middle;
hinge line longer in proportion to the shell. The similarity of form in these two shells which
are really distinct, renders it a matter of interest to ascertain the relative position of the Swe-
dish, English and American species, and whether the former may not be identical to the larger
one here mentioned.
14*
108 GEOLOGY OF THE FOURTH DISTRICT.
The Orthis striatula of the Trenton limestone differs from this shell in the less convexity
of the lower valve, and in the more strongly marked radii which are crenulated, or crossed by
elevatedlamellae which extend across the depressions between them; the beak is less incurved
and the shell more circular in form. -
Localities—Niagara, Lockport, Sweden, Rochester, Wolcott.
7. a. b. c. Orthis hybrida. Silurian Researches, pl. 13. f. 11. Lenticular, radiated; radii
dividing towards the margin, lower valve most convex; upper one slightly depressed in front;
front rather straight or a little impressed; area narrow; hinge line short.
The specimen figured is somewhat larger than the one in the Silurian Researches, but the
more abundant form is like that. It is usually convex near the beaks and flattened toward
the margin, the valves appearing equal. The shell occurs with O. canalis and the other forms
here figured, few of them rising above the shale of the Niagara group, and none of them
known above the Niagara limestone. *
Locality—Lockport, Sweden, Rochester and Wolcott.
Atrypa affinis. (Terebratula affinis, M. C. t. 324, f. 2.
A. reticularis, DALMAN, HISINGER, &c.)
The illustration presents the common form of this va-
riable species as it occurs in the shale of the Niagara
group. The shell is marked by about twenty-four radii
which bifurcate about one-third of the distance from the
beak to the margin. The whole surface is closely imbricated by the projecting laminæ of the
shell. This structure is visible in the enlarged portion. - -
This shell is common in all localities and abundant in many places. It is usually much
flattened, rarely presenting the rotund form of the figure. Several other species of this genus
are common in this group, and some of them will be figured at the end of the volume.
1. Orbicula? squamiformis. - - 3. Orbicula corrugata.
2, Lingula lamellata. 4. Avicula emacerata
1. Orbicula 2 squamiformis, n. S. – Oval, depressed; apex nearer to one extremity of the
shell; surface covered with concentric lines, which diverge on the posterior part of the shell.
Shell translucent. Longest diameter sº of an inch.
NIAGARA GROUP. 109
This fossil corresponds very closely with the Patella? implicata (Silurian Researches,
p. 625, pl. 12, f. 14, a.). I had supposed it to be the young of fig. 3; but its oval form, and
the lateral situation of the apex, preclude the idea. It occurs on the surface of the shaly
laminae with other fossils, always presenting the appearance of a thin translucent scale.
Locality—Rochester and Sweden in Monroe county.
2. Lingula lamellata, n. S.–Oval, somewhat broader towards the base. Shell covered
with concentric, slightly undulating, elevated lamellae, wrinkled at the sides, gradually rounded
at the base. Beak sharp, scarcely elevated. -
Perfect specimens of this fossil are not of common occurrence. The surface is not striated,
but the shell appears as if composed of concentric laminae with elevated edges.
Locality—Lockport, Rochester, Sweden.
3. Orbicula corrugata, n. S. — Orbicular ; surface strongly wrinkled, and covered with
finer concentric undulating lines; muscular impression on the under valve very distinct, and
often extending half way from the apex to the circumference.
This fossil is easily distinguished from any other in the rock, by its orbicular form and
wrinkled surface. I have seen one or two specimens which exhibit the two valves only par-
tially separated, and there seems no doubt of the propriety of its reference to this genus.
Locality—Rochester, Sweden, Lockport, Wayne county. -
4. Avicula emacerata (CoMFAD, Jour. Acad. Nat. Sci. Vol. 8, p. 241, pl. 12, f. 15). —
Lower valve slightly convex, wider than high, finely radiated; radii equal, diverging toward
the margin, crossed by elevated concentric lines, giving the whole surface a cancellated ap-
pearance. Upper valve smaller, nearly flat, plain, or with a few concentric lines, and some-
times a few radii on the posterior wing; posterior wing acutely angular; anterior one slightly
rounded at the extremity, very short. -
From some specimens, it would appear that the radii on the larger valve become obsolete
with age, as several large valves have been seen without them.
Locality—Lockport, Sweden. 39 3
* : * * * : -º
º, A. \\\\ º: .
޺
º
Ž
*
|
:
3
**º:
º º W
* Sº §sºs
Mº
§
º, - § Y.
N - * *
§§§
wº -
1 and 2. Euomphalus hemisphericus. - 3. Cornulites arcuatus.
110 GEOLogy of THE FOURTH DISTRICT.
1 and 2. Euomphalus hemisphericus, n. S. – Convex, hemispherical; volutions about four,
crossed by striae and elevated lines of growth. - - -
This fossil usually occurs as a cast in the Niagara limestone, and consequently the charac-
ters of the shell are not perfectly known.
Localities—Rochester and Lockport, in limestone.
3. Cornulites arcuatus (ConRAD, Jour. Acad. Nat. Sci. Vol. 8, p. 276, pl. 17, f. 8). —
Conical, rapidly attenuated ; composed of a series of cup-form disks, placed above and in-
serted within each other at the margins. - -
The annulations are more rounded than in C. serpularius of the Wenlock limestone (See
Silurian Researches, p. 627, pl. 26, f. 5). It is easily distinguished from any other fossil in
the group, or even in the system. It occurs in single specimens at Rochester in the lime-
stone, and at Lockport in groups, in cavities which are partially filled with spar. The fossil is
usually nearly destroyed, its form being left invested with crystals, and sometimes a small
central tube or siphuncle? is all that remains.
40.
1. Orthoceras annulatum. - t 2. Conularia quadrisulcata.
1. Orthoceras annulatum?–Very gradually tapering; ornamented with transverse rings,
and numerous undulating lines; siphuncle central. Diameter 1 # to 2 inches.
In many respects, this resembles the figure of O. annulatum (Silurian Researches, pl. 9,
f. 5); and more nearly the figure of the same in Mineral Conchology, t. 133; but it is de-
stitute of longitudinal furrows or arched laminae. Since, however, that species is variable in
its characters, it may be the same. The specimen figured is a flattened fragment from the
NIAGARA GROUP, 111
shale, and is one of the ordinary fossils of the group, being found in all localities. In speci-
mens from the limestone, the annulations are stronger and more acute. f
Locality—Lockport, Rochester, Sweden, Clarendon, in shale and limestone.
Several other species of Orthocerae occur in this group, among which are forms closely
resembling, if not identical with O. virgatum (Silurian Researches, pl. 9, f. 4), or O. undu-
latum (Mineral Conchology, t. 59), and O. imbricatum (His. Pet. Suec. p. 29, t. ix, f. 9;
and Silurian Researches, pl. 9, f. 2). -
2. Conularia quadrisulcata? (MILLER, M. C. t. 260, f. 3 and 4 ; His. Pet. Suec. p. 30,
t. x, f. 5; Silurian Researches, p. 626, pl. 12, f. 22). — Conical; crossed by obliquely
transverse furrows and ridges, which are not always equal. The ridges are finely and beau-
tifully crenulated, and the furrows crossed by grooves which are a continuation of the spaces
between the crenulations of the ridges. Shell compressed; in shale, much expanded, and
larger than specimens usually figured. It is ordinarily found in fragments of a much smaller
size. - - - -
Since the character of the surface is so similar in this and other species, it is not improbable
that several have been confounded under this name.
Locality—Lockport, Rochester.
CRINOIDEA.
The species of this family appear to have been more abundant in this group than in any
other in the State; and there are probably as many species, well identified, from the Niagara
shale, as from all the other rocks of the New-York System. An explanation of their structure
will be found in another place; nothing more being intended in these illustrations, then to
present the usual appearance of the fossil. *-. - -
41.
§3 ºx Rºssºsº
;%;º
#/ft unw
§||
tººgº
- |
§ § § % §.}} º ºft-
§ § º #5 § © § gº º # \º- ... s -
§ R. e º ºn 1 We ..!º-
§ ſº º Mº- yº.
§ º § wºn, M M\º:
§ º W W.
º º, i.
f Alſº
º
º § #||
*ś º
1, 2. Caryocrinus ornatus. 3. Cyathocrinites pyriformis,
3
I 12 GEOLOGY OF THE FOURTH DISTRICT.
1, 2. Caryocrinus ornatus (SAY, Jour. Acad. Nat. Sci. Vol. 4, p. 289). — This fossil
usually occurs separated from the column, and destitute of arms or tentacula. From its sphe-
roidal form, it has received the name of “Petrified Walnut.” It is composed of plates which
are tuberculated on the surface, having generally a double row of larger ones along the line
from the centre to each angle of the plate. The dark lines in the figures indicate the junction
of the plates. The points of attachment of the arms are visible near the top of the specimen.
Fig. 2 is a view of the base, presenting the point of attachment of the column, the form of the
pelvic plates, and the bases of the costals. Separate plates are often met with, and they may
always be known by their strongly tuberculated surface. - -
This fossil occurs in great numbers at Lockport, and in many instances covered by a coral
which had grown upon it after the destruction of the former, as is evident from its often co-
vering the point of attachment of the column and arms, and closing up the aperture on the
crown. - -
The C. loricatus of Say, was probably a specimen which had undergone some modifica-
tion in the form of the plates, from injury or otherwise, a circumstance apparently not un-
common among the Crinoidea. - r - -
Locality—Lockport, and more rarely at Rochester and Sweden.
3. Cyathocrinites pyriformis (Silurian Researches, p. 672, pl. 17, f. 6. Ichthyocrinus
lavis, CoNRAD, Jour. Acad. Nat. Sci. Vol. 8, p. 279, pl. 15, f. 16.)—This species is known
by the great width of the plates near the base, which unite laterally, and divide in ascending
until they form the arm divisions; the latter fold inward toward the centre, sometimes nearly
closing. The upper part of the column is very slender, and composed of thin plates, which
join by a suture formed by the elevated lines which radiate from the centre. The surface is
faintly ornamented. - -
From the many specimens seen, which vary in form and proportions to a considerable de-
gree, I have no doubt of the identity of the fossils figured by Mr. Murchison and Mr. Conrad.
Locality—Lockport. - -
NIAGARA GROUP. 113
H
#
E.
šºë.
1. Hypanthocrinites caelatus. 3. Hypanthocrinites decorus.
2. Hypanthocrinites decorus. 4. Marsupiocrinites (!) dactylus.
1. Hypanthocrinites calatus, H.-Pelvic plates 5, hexagonal, equal in size, supporting on
their upper edges five quadrangular costals, resting upon the superior lateral edges of the
pelvic plates, are five large (nine-sided) intercostal plates. Each costal supports a nearly re-
gular pentagonal scapular plate, resting upon the upper oblique lateral edges of which, and
the intercostal plate are two pentagonal arm joints, and upon each one of these rests a some-
what quadrangular hand-joint, which supports two fingers composed of thin plates joining in
the centre by their cuneiform edges producing a longitudinal suture. Upon the superior edge
of the intercostal plates rests a double, somewhat conical plate, supporting a longitudinal rib,
which separates the pairs of arms and fingers. There is a similar single conical plate resting
on the superior lateral edges of the arm joints, and supporting in like manner a longitudinal
rib. These apparent ribs are partitions or dissepiments, which reach nearly to the centre,
separating the internal part of the crinoid in ten cells or compartments.
This species bears a close resemblance to the next, but differs from it in the following par-
ticulars: The whole structure is smaller, the plates are covered with tubercles or tubercu-
lated undulating lines; the arms are deeply sculptured or corrugated, so as to render the su-
ture almost invisible. The single conical plate supporting the rib is not truncated below, and
GEOL. 4TH DIST. 15
114 - GEOLOGY OF THE FOURTH DISTRIGT.
does not rest on the scapular. It is plainly referable to this genus of Mr. Phillips, and to
the genus Eucalyptocrinites of Goldfuss, as it is impossible that the figure which he repre-
sents, pl. 64, f. 7, should have had no column. The plates which Mr. Phillipºdescribes as
costals are in fact the pelvic plates, as can be plainly seen in the specimen here described,
the upper portion of the column still remaining enclosed.
Locality—Lockport, Sweden, Monroe county.
2 and 3. Hypanthocrinites decorus. (Silurian Researches, p. 672, pl. 17, f. 3.)—The
description of the last corresponds with this except in the few particulars noticed. This is
apparently the fossil described by Mr. Phillips. The ribs, however, instead of being rounded
and elevated toward their upper extremities, as there represented, are grooved (as in fig. 2,)
with a few slight tubercles, as if fitted for the attachment of some muscle or integument.
(This may possibly arise from an exfoliation of a part of the rib.) The tubercular plates
surrounding the mouth are not seen in the specimens figured, though they are in others. Fig.
2 represents the upper portion, which is broken off just above the plates, presenting a view
of the internal cavity beneath. - -
Locality—Lockport.
4. Marsupiocrinites?" dactylus, HALL. — Pelvic plates five, pentagonal,f slightly recurved
at the base; first costals five, pentagonal, supporting five hexagonal second costals; inter-
costal plates five, equal, and regularly hexagonal, resting on the superior lateral edges of the
first costals, Scapulars five, pentagonal, resting on the superior edges of the second costals,
and supporting upon their superior lateral edges two obliquely cuneiform hand joints; inter-
costals(?) ten, somewhat unequally six-sided, resting on the superior lateral edges of the se-
cond costal and intercostal plates. Upon the inner superior lateral edge of the interscapular
plate rests one edge of the hand joint, and upon the superior edge rests the base of the second
hand joint, which supports a finger composed of a double series of plates, uniting by their
lateral cuneiform edges, producing a longitudinal suture in the finger. The fingers are ar-
ranged somewhat in pairs, and separated by a cuneiform plate which rests upon the edges of
the hand joint. Between each pair of arms are two plates, one pentagonal, and the other
minute, quadrangular, both resting on the superior lateral edges of the interscapular plates.
The upper figure represents very clearly the structure of this crinoid; the plates are
slightly ornamented on the surface, and joined at the edges by a suture. The column is
composed Öf a double series of plates, one extending beyond the other, and are ornamented
on their edges.
Locality—Lockport.
* This fossilis provisionally referred to this geuus of Mr. Phillips, though it will probably require to be separated.
# They are represented in the wood cut as triangular, but the lateral edges join, forming a short side.
NIAGARA GROUP.
115
COR ALS.
Numerous forms of this class of fossils occur both in the shale and limestone. Few of the
solid or stone building corals are seen in the shale, its forms usually being referable to Rete-
pora, Fenestella, and genera of similar structure. There are also some other forms of this
|
||||||}
|
ſ
class of fossils, which appear referable to the corticiferous polyparia.
| º
\ \\
º
º º
* | |
* | |
*
º liſ
§: \ º
º ſ ". | |
º
*||
º º
§§
§ §§ | |||}||||||
º |
§ º *
º º º º
l
º
º
º \\ l
[] º tººl
- §§ |
º sº |
|| || jº
º jº
|
|W §§ W
º ſº º Aº
$º |f|, |\\\\\\\\\ }
ºffs
ºff,
º \\lišlij
iº (\#||
jº º i | ||
ſ
º
j}:
#| ||
§ --- !ºl [. § *:
º
|
||
|
|
|
|
t
|
f
D
º
§
jºiſſ."
ji; j
t
§
º
:
;
;
|
º
lift
ºji
i
-W;i t§li
i#-
º-º
§-A.
*º§
K.§
§º:
§:
§|W
§s:
5:
||-
;|:
ſ|t
||
|
W
\
#|jà
sº |
§
|
º
\\ººl
§ º
sº
º
§
|
\
º
§ |||
º
#! §
| § § tº
|# º \\
| § i; §§ º
§§ i. jº
º
|
| |
º: | - - jº Nº.
*i; º
#|º
sº
º
º
º
§
\
|
º
ſ
t
º º
|
W
l
|
º
§
\\
\
|
\
N
illiº!
j||
º
º
º
§§§ {\\\\\\\ {||&
Wilſº |
|
§§ §
tº: §.
àºjī. it. |
º §º º º º
- º
|
tº º
* > *
1. Gorgonia? reteformis. No visible axis; branched or expanding from a centre (axis 7);
branches flattened, wrinkled and indistinctly striated, anastomosing so as to form a reticulated
structure; no visible pores or papillae.
In general appearances this fossil closely resembles Gorgonia assimilis, (Silurian Re-
searches, pl. 15, f. 27,) to which I had referred it. There is, however, no solid axis, a central
point or depression being visible, from which the coral expands. It is probably the same as fig.
28, ut supra. The figure is from the central portion where the margin is destroyed. I am
indebted to Dr. Fassett of Lockport for a perfect specimen, six inches in diameter.
I have
another imperfect specimen where the margins are destroyed, and which must have been
18 or 20 inches in extent when perfect.
It occurs in the shale at Lockport, usually in fragments.
2. Gorgonia 2 Expanding from a base or point of attachment, branched; branches bifur-
cating as they ascend, slightly diverging and united at intervals by slender filaments. The
whole forms a delicate and beautiful expansion, often extending over several inches. Its
perfect form is unknown. No pores are visible, and both this and the preceding species
present merely a film of carbonaceous matter. They are provisionally referred to Gorgonia,
and if not strictly belonging to that genus are closely allied.
15* |
116 GEOLOGY OF THE FOURTH DISTRICT.
§§ ſº Aſ
§). l -
f \ \ ſº
§§§ -
º º WN º º º
º \\ 9 ſº
# \, . " º ſ ſº
§§§ º %
sº - * %
§§
§§
§§
\\ .
- \\ Ø
§§ 4% º
§Aſſº’ iſ \|
.* \\ % ſ \
º | % | \\ ſº
º
|
!
|
º
wt
º
|
/
d%
;
§
|
|º
º
W
\
1. ? This fossil is completely flattened, presenting no solid substance, except a
thin carbonaceous film. It appears like a collection of fine hairs arranged obliquely on a
central axis like the tail of some animal. It resembles in structure some of the solid corals
where the pores are oblique to the direction of the axis, but here there is no defined margin,
and the calcareous matter, if ever existing, has been removed.
2, 3. Coral resembling Isis. This fossil has a calcareous stem and the external structure
is much like some of the recent corals. Figure 2 represents the natural size, and fig. 3 is a
portion magnified. It is the only coral presenting this structure which I have met with in the
New-York rocks. It occurs at Lockport, with the last, in the shale of this group.
Since there are numerous corals in this shale still retaining their calcareous character and
some of the expanded or net-like forms, which are always clearly referable to structures of
this kind, it seems natural to infer that those forms where only a thin carbonaceous film
remains, with no visible pores, or structure like the stony corals, should be referred to some
other division of the Polyparia at least, and perhaps even to some of the more gelatinous
or less solid forms than Gorgonia. -
The fossils figured in the preceding wood cuts with the exception of two or three species,
are, so far as known, confined to this group. From the identity of many of these with forms
described by Mr. Murchison, from the Wenlock shale, and limestone of England, we have
inferred that the Niagara group of New-York represents, to a considerable degree, that for-
mation. Though the Wenlock limestone contains some forms identical with those of the
NIAGARA GROUP. - 117
lower limestones of the Helderberg division, which in New-York are separated by the Onon-
daga salt group One thousand feet in thickness, yet we can account for this apparent difference
upon the supposition that the latter formation does not exist in England, and that the higher
limestones come down upon the lower, or equivalent of Niagara, and the whole are recog-
nized as one formation, as the same are in Ohio and the southwest. -
The fossils common to the two formations can be seen by the references in the descriptions;
they are: Strophomena transversalis, S. depressa, Orthis canalis or O. elegantula, O. hy-
brida, Delthyris radiatus, D. sinuatus, Atrypa affinis, A. imbricata, A. cuneata, Conularia
quadrisulcata, Bumastis Barriensis, Homalonotus delphinocephalus, Hypanthocrinites de-
corus, Cyathocrinites pyriformis. - - -
These are the principal forms though there are several others which are very similar if not
identical to those figured in plates 12 and 13 of the Silurian Researches. The occurrence of
so great a number as here given, and which with two or three exceptions are all confined to
this group, leaves no doubt of the perfect identity of these formations whatever may be inferred
of others. - - -
12. ONONDAGA SALT GROUP.
Calciferous slate, OT Second greywacke with Shell limerock, of EATON (Canal Rocks, p. 124).
Gypseous marls and slates (Annual Reports).
[M. of Woodcut, page 27.]
Succeeding the Niagara group, we find an immense development of argillaceous shales and
marls, with shaly limestones, the whole embracing veins and beds of gypsum. The general
aspect is a light ashen, or approaching to drab color, with some portions of dull bluish green.
The lower part is of deep red with spots of green, very closely resembling some of the more
shaly portions of the Medina sandstone (as before described at Lewiston and other places).
Succeeding this, where penetrated beyond the reach of atmospheric influences, the rock is
greyish blue like the ordinary blue clays, with bands of red or brown. This portion and that
succeeding it are often greenish and spotted, and contain seams of fibrous gypsum, and small
masses of transparent or reddish selenite and compact gypsum. From this it becomes gra-
dually more greyish or ash-colored, with thin strata of argillaceous limestone, which is some-
times dark, though generally of the same color as the mass around. The whole terminates
upward by a grey or drab limestone, called by Mr. Vanuxem the Magnesian deposit.
This group receives its name from the great development of the products in the county of
Onondaga. In an economical point of view, this is one of the most important groups in the
system; containing all the workable beds of gypsum in Western New-York, and giving rise
118 GEOLOGY OF THE FOURTH DISTRICT.
to the salines from which nearly all the salt in the State is manufactured. It extends east
beyond the limits of the district, and west beyond the Niagara river into Canada; maintaining
the same general characters, and containing beds of gypsum. Some of the shaly and porous
limestones of the upper part of the group appear still beyond, forming the island of Mackinaw,
if we may judge from similarity in character, though the connexion with rocks above or below
is not there visible. Its resources, except in certain places, are at this time undeveloped;
and it is only when its limits and extent shall become known, that its immense value will be
appreciated. - -
From the character of the group, it has been deeply excavated by the ancient denuding
agency, and it occupies a depression throughout the greater part of the Fourth District; while
from the accumulation of drift upon its surface, and the absence of deep streams, there are
few points where good sections can be obtained. The absolute contact of this group with the
one below has nowhere been observed in the district; yet from the small space intervening,
and no rock being known in this place, there remains no doubt of the order of succession.
In the Third District, its connexion with the Niagara group is seen in several places, both
together being exposed in the banks of ravines. -
Localities.—By reference to the Geological Map, it will be seen that this group occupies
the southern part of Wayne and the northern part of Ontario and Seneca counties; the
southern part of Monroe county extending southward for a short distance into Livingston on
the Genesee river; the northern part of Genesee and Erie counties, and a small portion of
the southern part of Niagara. Its greatest width in the district is at its eastern extremity,
where the denudation of the higher rocks give this formation a greater southern extension by
several miles than it has farther west.
The best section of the group which I have been able to obtain, is along the country south
from Rochester. The lower portions are developed only at a few points, but their characters
are known from several borings which have been made to great depths for the purpose of ob-
taining water. The higher portions of the group with the gypsum beds and the porous lime-
stone are exposed on Allen's creek at Garbutt's mill. Trom these observations the following
section has been constructed. t
ONONDAGA SALT GROUP, - 119
f. Terminal mass of the deposit, which is a light grey or drab-colored impure limestone, with cavities sometimes con-
taining crystals, and often embracing shaly beds.
c, d, e. Shaly and compact impure limestones, with shale and marl, embracing two ranges of plaster beds. Between the
two ranges of plaster beds is a bed of shaly limestone, d, with some imperfect hopper-shaped cavities, and a
harder grey limestone, with numerous pores, sometimes very minute.
6. Green marl and shale, with some shaly limestone, containing veins of fibrous gypsum, selenite, and small nodules of
gypsum.
a. Green and bluish green shale, with bands of red.
There are no well marked lines of division between the different portions of the deposit 3.S
here enumerated, but each one taken as a whole is sufficiently well characterized.
1. The red shale forming the lower division of the group, and so well developed in the
Third District, I have not been able to find west of the Genesee river. It appears in the
eastern part of Wayne county, as indicated by the deep red color of the soil which overlies
it. At Lockville the greenish blue marl with bands of red has been quarried from the bed
of the canal. - *
West of the Genesee this is the lowest visible mass; the red shale has either thinned out
or lost its color, gradually becoming a blueish green; while otherwise the lithological cha-
racter remains the same. On first exposure it is compact and brittle, presenting an earthy
fracture; but a few days are sufficient to commence the work of destruction, which goes on
till the whole is resolved into a clayey mass. -
Since a deoxidation of the coloring matter of the red shale would produce the green color
of the lower mass as developed in the Fourth District, it is, perhaps, not improbable that this
cause has operated on a large scale, changing the color of the mass by the same process
which has produced the green spots and bands in the same rock farther east. -
The green marl of the lower division appears near the canal at Fairport, and again at Car-
tersville. On the west side of the Genesee this portion appears on the surface in but few
places. The bed of the stream at Churchville exposes the greenish blue marl, and in dig-
ging a well at the same place this was found at a depth of thirty feet below the surface.
About one mile southeast of Churchville, at Wiley's mills, the green marl is seen in the bed
of the stream. At this place it embraces one or two thin strata of impure drab-colored lime-
stone. These localities are near the northern margin of the formation, the limestone being
120 GEOLOGY OF THE FOURTH DISTRICT.
visible within a short distance on the north side of Black creek. In an excavation half a
mile east of Churchville, some loose masses of the Niagara limestone were found, but no
rock of this group. I
In the northern towns of Genesee county, the lower portion of this group were seen in se-
veral places, mostly however as excavated from wells. The depression along the line of the
Tonnewanta creek, which is near the northern margin of this formation, prevents any expo-
sure of the rock. Along the whole distance to the Niagara river, the surface is deeply co-
vered by drift, and it is only in a few points or from artificial excavations that the mass
becomes visible. -
2. The prevailing features of the second division of this group are a green and ashen marl,
with seams of fibrous gypsum, and red or transparent selenite, and often embracing nodules
of compact gypsum. This occurs in the vicinity of Lyons, and at numerous points farther
west. It crops out on the road some distance northeast of Newark, and at Lockville it has
been excavated from the bed of the canal for the construction of the enlarged locks. Here it
contains seams and small irregular masses of reddish lamellar gypsum. Its general charac-
ter at this place is a greenish grey compact argillaceous marl, which crumbles rapidly on
exposure, and forms a tenaceous greenish clay. Near Newark the mass is variegated with
red, and red spotted with green, and some portions are of a light ashen color. It is marked
by the presence of reddish and transparent lamellar gypsum, and seams of fibrous gypsum.
The same occurs farther west, and is seen in the banks of the canal near Palmyra.
Thence to the Genesee river it is scarcely seen upon the surface, but has been found in
digging wells.
Westward, we find the same rock in Bergen, Byron, Elba and Alabama, in Genesee
county. About one mile north of Bergen Centre the greenish gypseous marls are excavated
along the line of the railroad. In digging wells in the same neighborhood, these marls with.
fibrous gypsum and selenite are usually encountered, and it generally requires that they be
penetrated to a considerable depth before a permanent supply of water can be obtained. This
character is the prevailing one through the counties of Monroe and Genesee.
There are few points where a natural exposure of these rocks can be obtained, and it is
principally from artificial excavations that we have any knowledge of their character.
Throughout its whole extent in Erie county, there is scarcely a natural exposure of the
rock, and the depth of the drift is so great that it is only in a few points that excavations
have been made to any considerable depth below it.
3. The third deposit embraces all the gypsum beds of the district which are of economi-
cal importance. Although this mineral occurs in the deposit below this, as before stated, in
seams and small nodules, yet it has never been discovered in quantities of any importance,
and there is no probability that much will be found. The greater part of this division con-
sists of grey or ash-colored marls and shales, with thin bedded shaly limestones, which are
usually of the same color, though sometimes much darker.
ONONDAGA SALT GROUP. 121
Owing to the deep denudation in the direction of Seneca and Cayuga lakes northward, the
whole group has been removed to so great a depth as to offer no evidence of its existence.
Along the line of the Erie canal, the middle division appears a short distance before reaching
Clyde. The third division, with the higher range of plaster beds, appears at Seneca falls,
and along the outlet of the lake for three miles eastward. Extensive beds of gypsum are here
exposed in both banks of the gorge, the largest on the north side. The surrounding mass is
a light ashen friable marl, with a few thin strata of impure limestone towards the top. Where
exposed alone, it has the character of a loamy clay, containing some carbonate of lime; and
in the vicinity of the masses of gypsum, contains some of that mineral disseminated through
it. The enclosed masses of gypsum are somewhat conical, though often irregular from the
encroachment of the enclosing rock. The marl and gypsum are both stratified, the lines of
division in the former often extending through the latter. There is usually a considerable
admixture of earthy matter in the gypsum, and it appears as if segregated from the mass
during its consolidation, by a well known law of attraction among particles of the same kind.
The following woodcut is an illustration of the largest mass seen along the outlet below
Seneca Falls village, and gives the usual appearance of the beds of the upper division, as
exhibited in the Fourth District:
cº-º-º-º:
8------ - -º-
45. -
* º
1. Compact granular gypsum, with lines of stratification.
2. Soft decomposing gypseous marl.
3. A lateral extension of the bed, with a greater admixture of argillaceous matter.
Along the outlet of Canandaigua lake, in the town of Phelps, we find a good exposure of
the higher range of plaster beds. The general appearance, and the character of the succeed-
ing masses, are like the same at Seneca Falls. The marls are mostly ash colored, with a
few strata of more siliceous character which are bluish. The only beds explored are those
[GEoL. 4th DIST.] 16
122 GEOLOGY OF THE FOURTH DISTRICT,
appearing in the banks of the outlet, though it is known to exist farther north. On the south.
side of the outlet, there are several beds worked near the stream. The higher groups of the
Water-lime and the succeeding limestones limit the extent of this deposit within a distance of
half a mile to a mile south of the outlet. Few beds have been opened west of this town along
the outlet, though several are exposed. The principal beds in this neighborhood, are those
of Mr. Hildreth, on the south side; Norton & Co., Wandemark & Co., Cook, Robinson and
Wanderhoff, on the north side. - .
Some of these quarries present interesting features not noticed elsewhere. The following
illustration is of Norton & Co.'s quarry, and Vandemark's presents nearly the same appearance.
46.
G. Beds of Gypsum, as exposed in the face of the bank.
a, a. A thin stratum of tough silico-argillaceous limestone, extending through the plaster beds, and continuously through
the adjoining rock. -
b. Soft shale or marl, filling the spaces between the beds of gypsum.
c. Two feet of compact, and slaty limestone, the harder portions with irregular cavities.
d. Six feet soft greenish shale. -
The continuation of the impure stratum of limestone through the beds of gypsum, renders
this an interesting exposure. The beds are likewise divided in the same way by a layer of
slaty limestone at the line represented as the base of this diagram, and below this the gypsum
continues to the depth of seven feet. These occurrences prove the manner in which this mi-
neral has been segregated from the surrounding rock. The softer portions of the marl readily
gave way for the formation of these masses, which were more strongly attracted together; on
the other hand, the shaly siliceous mass, which continues through the beds, seems to have
possessed attractive force equally with the particles of gypsum, thus maintaining its position
while the softer portions were displaced.
Almost all the gypsum effervesces with acids, showing the presence of carbonate of lime,
and its dull earthy color is owing to admixture of argillaceous matter. The beds of gypsum
are usually horizontal at the base, resting on the same kind of marly deposit as that above.
In a few instances, the base is irregular or undulating, resting on an uneven bed. The illus-
tration No. 47 presents an example of this kind, where the marl rises above, and the base is
partially enclosed in the gypsum. -
ÜNONDAGA SALT GROUP. 123
s
47. §:
---…-:=:
* :=rssºciº===º-º-º-º-º-º: sm as sº as sesaº an º ºs as
- ºº::====EE
E===s+:F-Fºr; -
- v-
•-ºm-º-º-º-
-------E
----->
The strata are slightly undulated, always rising gently towards the mass and descending
from it. This is doubtless caused by the nature of the two substances and their comparative
power of resisting atmospheric and other agencies. The gypsum is compact and little affected
by air or moisture, while the numerous seams of the surrounding marly and shaly mass
freely admit water, which, from the soft and yielding nature of the rock, gradually removes
portions which are carried off in the outlet of the springs and streams, thus diminishing the
quantity, and causing a slight sinking down between the beds. The illustration No. 48
exhibits the usual appearance of the strata in these situations.
*~~
E=º w ºfflºšºse:grayºs * , , º, …-º tº-º-º:
======###############$ºśs=º:
º-º-º: º-º-º: C- - º-ºr- - *::::::º
C-3 E::::::::::: sº-º ######### º::::::::===
*::::::::B; ºffl ----------
: #=#: :=E::::::::=: -º-º-º-º-º-º-º:
* 25? #: ####:Fºº E.########### ==
ññāmā; ################
Wºlſº | |||ſſiń §§
ºfflº"lºº" ſºlºiſſºl
------------ - w - -- #E *:::::: §º §:#$º
º: ==
The enclosed bed of gypsum exhibits a more continuous character than usual, presenting
three conical or dome-shaped elevations, separated by the nearly horizontally stratified marl.
The lower range of beds, as seen in Monroe county, are nowhere known in this part of the
country. At Seneca falls the soft marls are succeeded above by some harder layers of im-
pure limestone, with irregular cavities which are lined with calcareous matter, in mammillary
forms, evidently a recent deposition from solution. Connected with these strata, and just
below, are some small masses of dark colored, crystallized gypsum, in stellated forms.
These porous layers are succeeded by a darker and more pure, compact, brittle, limestone,
which is the highest rock visible at this place. This would appear to be the terminal deposit
- 16* |
124 GEOLOGY OF THE FOURTH DISTRICT.
of the group, but it is not marked by the striated or columnar appearances usually seen, and
the irregular cavities which are sometimes lined with crystalline substances.
South and southwest of Newark, in Wayne county, the limestone separating the two ranges
of plaster beds is seen on the surface in several places, presenting an appearance as if cut or
hacked. These markings extend but a few inches continuously, and have two directions,
frequently crossing each other, and evidently partake of the nature of joints, the rock breaking
in these directions much more easily than elsewhere. This character is prevalent in that
portion of the group throughout the district.
At the locality just named gypsum, in small rounded masses, is found at some depth below
the surface, but it is nowhere quarried in this neighborhood. The surface presents, in a small
degree, what is more fully developed in Monroe county, being covered with small mounds or
dome-shaped elevations, caused by the sinking down of the strata between the beds of gyp-
sum. f
The rock surrounding the higher range of beds is usually more argillaceous than in the lower,
the latter being frequently a compact, slaty limestone, enclosing a small quantity of soft marl
immediately surrounding the mass of gypsum. It is probably owing to this character of the
rock that the lower gypsum beds are purer and more free from admixture of argillaceous
matter than those above.
In the Annual Report of 1839, it was stated that the gypsum (principally crystalline) near
Newark, the beds near Port-Gibson, and south of that point, and those on the Canandaigua
outlet belonged to three distinct ranges. There still seems good reason for treating them in
the same manner, the two upper ones belonging to the two regular ranges of beds, and that
near Newark being perhaps only a greater development of the second division of the group
which usually presents only thin seams or small nodules of this mineral.
Westward, along the Canandaigua outlet, there is little gypsum seen after leaving the town
of Phelps; though the rocks of the higher part of the group are still visible, even as far as
the point where the course of the outlet bends southward. West of this point, as far as
Mud creek, the great accumulation of drift does not admit any exposure of these deposits.
That they exist along this distance there can be no reasonable doubt; and more especially
since a bed of gypsum has been discovered near the village of Victor. This fact also leads
to another observation, which should be borne in mind as applicable to a large portion of the
country occupied by this formation east of the Genesee, and within the limits of the Fourth
District. Many of the hills apparently of drift or alluvial, and rising from fifty to one hun-
dred feet above the surrounding country, are in reality composed of outliers of these marly
deposits, with only a thin covering of the loose materials.
The same remarks made in reference to the western part of Ontario county, apply equally
to that portion of Monroe county on the east side of the Genesee. Although the gypsum beds
have not been found, there is every reason to believe that they exist beneath the superficial
accumulations. * * * : . - - -
On the west side of the Genesee river, the third division of this group, embracing the
ONONDAGA SALT GROUP. 125
two ranges of plaster beds, occurs on Allen's creek at Garbutt's mills. The upper part
of the section on page 119 is constructed from this locality. The lowest range of beds is
best developed on the north side of the creek, where the rocks are covered with only a
small depth of soil. The surface is raised into small rounded hillocks of a generally uniform
height, and with depressions communicating over a considerable space, giving the appearance
as of little mounds of earth. After removing the soil to a small depth, the rock appears, pre-
senting the same convex or rounded contour as the surface above. The strata are usually
thin, and present an appearance as if broken up by some elevating force from beneath.
Below the rock lies a spherical mass of gypsum, upon every side of which the strata dip
till they assume their original horizontal position. The proximity of these masses however
is often so close that the strata continue undulating, being depressed between and elevated
above the beds of gypsum. The woodcut below represents a section of two beds of gypsum
at this place. - -
The elevation and breaking up of the strata was doubtless caused in part by the expansion
of the gypsum during solidification, (it being more or less crystalline,) while the strata above
were partially indurated. In the lower beds, where the surrounding mass of rock is princi-
pally a soft marl or shale, no such evidence is perceived, except perhaps in a slight degree.
(See woodcut, page 123.) In this case the surrounding mass was probably in a yielding con-
dition at the time of the solidification of the gypsum, and consequently the particles of the
one gave place to the other, presenting no evidence of force. This is further proved by the
continuation of a semi-crystalline siliceous stratum through a bed of gypsum, while the marls
above and below, though doubtless originally equally continuous, have been displaced to give
room to the gypsum, which with a stronger tendency to concentration, has accumulated into
flattened spheroidal or low conical masses. Wherever the carbonate of lime was in such
proportion as to induce a tendency to crystallization, the strata appear to have become in
some degree consolidated before the gypsum ; on the other hand, where the proportion of
argillaceous greatly predominated over the calcareous matter, the tendency to crystallization
was lessened or entirely prevented, and the gypsum consolidated before the surrounding mass.
The same operations appear to have gone on here, as we often perceive in artificial com-
pounds, where the tendency to crystallization is much stronger in one body than in another.
These beds of gypsum are usually from four to eight feet below the surface; few being
worked at the latter depth, the expense being too great. There is sometimes an appearance
of a third range of beds, but this is not continuous. The rock above is so much broken as
freely to admit the surface water, and thus broad fissures are often worn in the softer marls;
and sometimes even in the mass of gypsum. -
126 GEOLOGY OF THE FOURTH DISTRICT.
The dome-shaped elevations are said by the inhabitants not to appear till after the settlement
and clearing of the country, and it is a general opinion that the gypsum continues to form at
the present time. It is even asserted that stone walls have been overturned, and the founda-
tions of buildings elevated by this process. Since the rocks must have become consolidated,
and the gypsum formed, long anterior to the settlement of the country, as is evident from
its appearance in the banks of streams, which excavated their channels long before the present
vegetation flourished, these apparent phenomena must meet some other explanation. In the
natural state of the country, the great accumulation of vegetable matter would prevent the
prominent appearance of these little mounds, even if they existed. Since, however, we know
that the surface water is rapidly drained off in these depressions, readily finding its way be-
tween the strata and through the fissures, it carries with it a small quantity of the soil, which
is repeated at every successive rain. As a natural consequence, the original inequalities of
the surface of the strata are gradually developed, and in some places the more elevated parts
become denuded of the soil which covered them. -
Beyond this point, there is a considerable space in the western part of Monroe county,
where no beds of gypsum are known.
In the north part of the towns of Leroy and Stafford in Genesee county, the lower range
of beds appear, and are extensively worked at a few places. There is no evidence of the
higher range of beds through these towns, or at any point farther west, and it seems probable
that they have discontinued. In this county, the second range appear to be as well developed
as elsewhere in the district. These beds are overlaid by the porous rock, which is so strongly
marked in the Third District; here, however, the pores are rarely larger than a pin's head, and
usually compressed. This character is well developed at several beds, though not so obvious
in all. The quality of the gypsum varies very much, the most easterly beds being very im-
pure, and if not protected from the weather, will soon crumble down. Farther west the
gypsum is more pure, and in some of the beds entirely free of foreign admixture, furnishing
a good material for hard-finished walls. The same appearance of the surface is presented
as in Monroe county, and it is sought for as an indication of the existence of the gypsum.
The masses are all more or less spherical, and the strata above are elevated and broken as
before described.
Throughout the whole width of Erie county, this formation is covered to so great a depth
with drift or alluvion, that there are only one or two places known where the rocks of the
lower divisions are seen. The principal point is on the farm of Mr. Martin, in the north part
of the town of Clarence. The rock is that portion coming between the two ranges of plaster
beds; it consists of several thin strata of limestone, with cavities of the size of flax seeds,
several often communicating, forming linear ones. A few incipient hopper-shaped cavities
were observed, but their forms were quite indistinct. Some portion of the rock here exposed
exhibits a tendency to a concretionary or contorted structure, presenting abrupt curvatures of
the laminæ, which could only have resulted after deposition. The surface of the strata
presents the appearance before referred to, as if hacked with an axe, being the result of a
weathering of the joints upon the surface. \
ONONDAGA SALT GROUP. I27
|
The porous rock indicating a position between the two ranges of plaster beds, occurs on
Grand island; and at a low stage of the river, fine specimens may be obtained. The group
extends beyond the Niagara, and appears on the Grand river in Canada.
In several places in Wayne and Monroe counties, imperfect hopper-form crystals and cavi-
ties appear in this portion of the group, but I have rarely observed them in Genesee or Erie
counties. The most perfect which I have seen, are at Garbutt's mill on Allen's creek. These
are, however, far from being as perfect as those of the Third District, figured in the report of
Mr. Vanuxem, from which the following illustration is taken.
#r
;:
W
Nº
=
Hopper-shaped crystals from the marl of the Onondaga salt group, town of Lenox, Madison county.*
The frequent occurrence of these forms in that portion of the group where the brine springs
exist, and their disappearance in a westerly direction, is in accordance with the views enter-
tained regarding their production. If the salines are dependant for their supply from the
solution of salt once filling these cavities, it appears futile to expect important brine springs in
situations where these do not occur in the strata. This might therefore furnish a guide to the
proximity of salt water; but since the formation is often deeply covered with drift, the springs
are usually more obvious than the hopper cavities. &
The small round or flattened pores before alluded to, usually occur in a layer above the
lower range of plaster beds, but I have occasionally seen some of them in a higher situation.
sº-
* Report of Third Geological District, p. 102.
128 GEOLOGY OF THE FOURTH DISTRICT.
This rock holds the place of the porous or vermicular limestone of the Third District, which
in many places closely resembles a vesicular lava. In the Fourth District these pores are
rarely larger than flax seeds, though sometimes several of them communicate with each other,
and not unfrequently they are filled with gypsum. -
The following illustration is from a specimen where the weathering has slightly enlarged
the cavities, and presents the common appearance of the larger pores. From this size, they
diminish till they become microscopic. º
£ tº: =######
#######
É===
|º3.
|
f
º
sº wº- - -- .*.*.*.* --
--- ſº 3 º'cºnºgrº-> Qº º ºs- -ºº:
-º-º- -- a sº- -º-º-º: * -*. - - ---, -ºº... . .
2. “cº-ºº: º §: º - bºº º - sº, º 'º
ºº::::::::::=º §º ſº
Porous limestone of Onondaga salt group.
In addition to the kind of cavities just described, we often meet with small linear ones,
which, in some parts of the shaly and marly limestones, are abundant. These are probably
produced, as in the Water-lime group, by the removal of crystals. For an illustration of these
forms, see the description of the Water-lime group in the following pages.
Fourth or Upper Deposit of the Group.
There is rarely any well defined line of demarcation between the shales and shaly lime-
stones of the last deposit, and this division. Still, however, it is often of considerable thick-
ness, and as a whole quite different from the rocks below. It is called by Mr. Vanuxem the
Magnesian deposit, from the striated or columnar surfaces like those described under the
Niagara group, page 95. These form a distinguishing feature, which does not appear in the
lower rocks of the group.
This division consists usually of thin-bedded impure limestones, drab or ash-colored, and
sometimes presenting a bluish tint on first exposure. The composition is that of a silico-
argillaceous limestone, and is the rock from which nearly all the hydraulic cement in the dis-
trict is obtained. From this circumstance, it has been distinguished as the Water lime, or
Hydraulic limestone, in the Annual Reports of the district. Finding, however, that the rock
ONONDAGA SALT GROUP. 129
distinguished as the Water-lime group in the Third District was a superior mass, and which
in the Fourth District contains no rock fit for hydraulic cement, the one in question is referred
to the Onondaga salt group, of which it forms the terminal division.
From being more enduring than the lower divisions of the group, it is more obvious, and
can be traced almost uninterruptedly through the district. In Seneca county, it does not appear
in its usual characters; the highest rock of the group being a fine-grained, dark-colored, and
greyish brown mass, which apparently represents the lower part of this division. Between
this and the succeeding limestone, there is an interval which is probably occupied by this mass,
but too deeply covered to be visible. It appears on the east side of Cayuga lake, coming
down to the lake shore. - -
Passing into Ontario county, we find this division much better developed, and possessing its
characteristic drab color. The mass may be traced almost uninterruptedly from near Oakes’
Corners in Phelps, to Manchester village. East of Vienna, all the strata of this division are
highly calcareous, and burned only for common quicklime. The principal quarries and kilns
are within one and a half miles of the village. It is also used for buildings and enclosures,
the layers being sufficiently thick. On exposure, it becomes stained with iron, and in almost
every locality is highly bituminous. -
At East-Vienna, this rock is burned for hydraulic cement, of which it is said to produce a
very good quality. Two miles farther west, at the quarry of Mr. Maffit, large quantities have
been used for this purpose. At this place the stone varies little, in external characters, from
that burned for lime. It consists of three distinct varieties: two only are used for the cement,
while the lower course is composed of thin layers of tough, argillaceous, bluish limestone,
which on exposure, breaks into small irregular fragments. This portion, on burning, melts
into a coarse porous slag, externally glazed and yellowish ; and in mineral characters, it is
precisely the same as the strata which pass through the gypsum beds on the north side of the
Canandaigua outlet. The second stratum consists of thin courses, externally drab-colored,
siliceous in texture, and harsh to the touch. This is succeeded by a few layers of unequal
thickness, lighter in color than those below, and much more calcareous. Of the two last
mentioned varieties, each at intervals partly takes the place of the other, so that the thickness
is variable, and the dividing line has an undulating direction. The depth of the two masses
together is from three to seven feet. If the lower of these is burned alone, the cement will
not “set” under water; and the upper burned alone is found to be too calcareous, and less
enduring than the more siliceous cements. To obviate the difficulty, both are burned toge-
ther, but without due regard to proportions. From the nature of the materials, it is evident
that the proportions of siliceous and calcareous matter must be very variable; and too little
attention has heretofore been given to this circumstance, and to the nature of the ingredients,
in the manufacture of hydraulic cement. - *
West of the last named quarries, the water-lime appears in numerous localities south of the
outlet, and near the road leading from Vienna to Manchester; but here it is used mostly for
enclosures, and at Manchester village for building stone, some of the layers being two or
three feet thick. It is too soft and argillaceous for hydraulic cement or good lime.
[GEoL. 4th DIST.] 17
|30 GEOLOGY OF THE FOURTH DISTRICT.
Above the village of Fredon this rock is seen in all its varieties for half a mile on Mud
creek; and along the line from Manchester to that village it approaches the surface and could
easily be obtained in any required quantity. Thence it extends west to the quarries in Men-
don, though the surface of the intervening distance is mostly covered with deep alluvium.
At Mendon the strata of this division are exposed in the bed of the stream below the falls.
There is also a quarry a few rods below the village, where the stone is wrought for build-
ings, step-stones, and other purposes. At Tinker's, near the west line of the town, this rock
crops out on the side of a hill, and it has been extensively quarried. This point offers a good
exposure of the rock; the strata are from half an inch to eighteen inches thick, generally
from four to eight. The higher layers for about five feet are thin and argillaceous, of a light
grey color. Eight feet below the surface is a bed which is very soft and porous, crumbling
rapidly on exposure to the air. The greatest depth penetrated is twenty-five feet; the lower
layers are the hardest, some of them having parallel seams of siliceous matter like agate, ex-
tending through them ; and all of them are more or less of this character. -
The vertical striated surfaces, supposed to be caused by the crystallization of sulphate of
magnesia, (the lignilites of Prof. Eaton,”) occur both in this quarry and at the village of
West-Mendon. These vary from a scarcely perceptible seam or suture in the rock to a
columnar mass several inches in length. In some instances these columns are curved as if
the action whatever it may have been, operated more powerfully on one side than the other.
The following woodcut illustrates an example of this kind, where a single fascicle is curved,
while the others in the same specimen are straight.
|º
w;
f;|
º
-º
|
\
- * * º sº
tº ºf illiºnſ.
§ {ſ; * | * * *
||||||#:
t - ſ: tº
|. - | ||}||3:
* . W
º, I' ‘.
#|| ||||||j,
º | | | º º:
#|| - |ill.i.
||5|| - #"
|*|| º ||||||}|
| i - |.
li.liº S. j.
º - º §:
| #| ||||||..
|; |||||||||||||:
#: º ||||}. #:
gº ºil ºr º º
|# 3. w |
|}}| º #
ſº -:
||||||||||
º ||f|||s -
|-|3|||}|.
|, | r | w º |.
|É. |||||||||||||||{{.
... . º º * | *
Mi'i II: ; - -
|||||
W |: . i. w
* “I. w A.
||fºº}: º | W
|||}|. -
|; : º
#| || :
," [. º: º
... tº "
|-}.}: º
airº
tºll ſ
º
*.§WJ.
Lignililes or Epsomités, Mendon, Monroe county.
These striated surfaces in this part of the salt group differ from those in the Niagara lime-
* Canal Rocks, page 134,
'ONONDAGA SALT GROUP. - 131
stone, in being more smooth, and I have never seen the insterstices filled with calcareous
matter. They are usually invested with a carbonaceous film, and present a black shining
surface.
The mode of formation in these bodies is supposed first to have been the crystallization of
sulphate of magnesia in the fibrous form, shooting up in the same manner as water sud-
denly congealed in a porous or spongy soil." Common salt will also produce the same ap-
pearance where the ground is saturated with it; and it would appear also that gypsum will
take the same forms, and present many of the same phenomena of these lignilites.f
The suture-like seams before spoken of usually occur as
horizontal lines of division, the striated surfaces vertical. In
the quarries at Mendon I observed some of these sutures in
a vertical position, and the striated surfaces parallel to the
place of stratification. The illustration represents the usual
appearance of these seams when on a small scale. These su-
tures sometimes separate, presenting a surface covered with
toothlike projections. -
They will be readily recognized by any one after seeing
these illustrations, and since they are known to be widely dif-
fused and occurring in greater or less perfection in nearly all
the calcareous strata of the system, and even in the higher
rocks, they have become subjects of interest. The great
limestone formation of the west, holding the place of the car-
boniferous of Europe, and apparently identical with that rock,
is marked by similar sutured divisions, and small columns like
wooden pins driven into the rock. -
After leaving Mendon, this rock is not seen on the east side
of the Genesee river; the first point west of the river where it
appears is on the “Street farm,” belonging to Mr. Wadsworth
of Geneseo. The lower part is composed of thinly laminated strata; the laminae often lighter
and darker in color, giving to the mass a striped appearance, which is very common at many
other places, and is one of those characters which serve to distinguish the rock at distant points.
The upper part is thick bedded, of an ashen color, and contains irregular cavities sometimes
filled with greenish clay; at others containing celestine, calcareous spar, and zinc blende.
The more compact portions of the rock have been quarried and used for structures on the
Genesee Valley canal. The following is the character of the strata as they appear at this
place; there is no connexion with any other rock visible either above or below.
Vertical suture in argillaceous lime-
stone, Mendon, N. Y.
* See Report of Third District, page 107.
# See an article in the American Journal of Science and Arts for Jan. 1842, by Dr. Locke, on some beautiful forms of
gypsum discovered in the mammoth cave in Kentucky.
1.7%
132 GEOLOGY OF THE FOURTH DISTRICT.
1. Irregular mass, much broken up by the denuding agency ........................ 3 feet.
2. Light drab or ash-colored limestone with irregular cavities ... . . . . . . . . . . . . . . . . . . . . . 4 “
3. Thick bed like No. 2, with cavities containing celestine, etc., slightly striped below .... 4; “
4. Consists of two strata, which are ash-colored and striped with darker; brittle after expo-
sure; siliceous. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 5 “
5. Thin-bedded, bluish, and striped with lighter colored; bed of quarry................ 4 “
About three miles farther west, at Caledonia village, the terminal strata are thin-bedded and
of a light drab color, and more argillaceous than in many other localities. The rock also
appears on the farm of Donald McKenzie, one mile north of Caledonia village, and at nume-
rous places along the brow of the terrace west of Mumford's mills. In some places the rock
is porous, or contains irregular cavities; in other places, it is compact and regularly bedded.
At Leroy falls, the whole thickness of this rock is exhibited, together with its connexion
with those below and above. The upper part is thin-bedded, in regular strata; the middle
consists of several thick strata; the whole of a light drab color.
At Morganville in Genesee county, nearly the same order of the strata occurs; the thick
beds are more siliceous than at Leroy falls, and they contain some irregular cavities. The
connexion of this group with the higher masses is well exhibited in the bed of the stream at
this place, while the fall is over the thick-bedded portions of the deposit under consideration.
By making examinations along the northern slope of the terrace which extends westward
from the Genesee, this rock may be seen in nearly every ravine or gorge which indents the
regular outline. It appears beneath the cherty layers of the corniferous limestone, two miles
north of Batavia. The thick-bedded portions form the falls of the Tonawanda on the Indian
reservation. At Falkirk in Erie county, this mass, capped by the corniferous layers, has
formed a fall and rapids of seventy or eighty feet. It again appears at Clarence Hollow, in
a few thin-bedded strata, with cavities lined with spar; and again at Williamsville, in thin
regular strata, which are burned for hydraulic cement. -
Three miles east of Buffalo, the same strata appear in the bed and banks of Conjockety
creek. The upper beds contain cavities filled with rhombic spar and sulphate of strontian.
Many of the smaller cavities which abound in the higher layer, are produced by the destruction
of a species of Turbinolopsis, casts of which sometimes remain studded with minute crystals.
At Black-Rock the higher strata of this deposit appear, having the same character as just
described. The Turbinolopsis was abundant at this place, and its casts remain partially
filling the small cavities. -
This rock is the product of a period intervening between the deposition of the great
mass of the salt group, which is mostly a mud deposit, and the commencement of the
limestone formations above. The character, therefore, partakes of the nature of both, being
an argillaceous limestone, with a small admixture of siliceous matter which probably resulted
from an intermingling of the materials which gave rise to the Oriskany sandstone, or a thin
deposit which seems to be its representative, and every where follows this rock in the Fourth
District. The ocean, which had been rendered turbid by the immense deposit of mud forming
ONONDAéA SALT GROUP, 133
this group, became gradually more clear, the supply ceasing, and at the same time the calca-
reous matter was furnished from another source, at first mingling with this, and finally giving
rise to an entire distinct formation, contrasting in the strongest degree both in lithological
characters and in the production of an immense number of organic forms.
While the deposit we have last considered forms a link, showing the gradual progress from
one to the other of these groups, the passage from the Niagara group to the Onondaga salt
group is abrupt, offering no gradation in character of products or in the continuation of fossil
species. So far as we know at present, throughout the whole western part of the State, no
trilobite and but two shells of the Niagara group reappear in any higher rock. The inter-
vention of the salt group seems to have exterminated them, and though limestones succeeded,
yet the same forms did not reappear, notwithstanding the circumstances appear to have been
favorable to the existence of many similar ones. -
From the sudden change in the nature of the deposit, and the great accumulation of mud,
it would appear that the Niagara limestone, which, from its abundance of corals, must have
been formed in a comparatively shallow sea, sunk down to a great depth, allowing this accu-
mulation above, of one thousand feet in thickness. Such a change, with the immediate repeti-
tion of a similar rock, could scarcely have happened, without some violent influence like the
breaking out of a mud volcano at the bottom of the ocean, by which this product was spread
rapidly and widely over its bed. The elevation of one point, attendant on such an eruption,
would naturally be accompanied by a corresponding depression of another, and this portion is
probably that upon which we have been making our investigations. This deposit, forming
the greater part of the salt group, is moreover unlike any other formation in the State, except
the marly portion of the Medina sandstone. The presence of large quantities of common salt,
sulphate of lime, and even free sulphuric acid, indicates an origin different from the geological
deposits forming the greater portion of the groups of the New-York System. The rarity of
fossils is another circumstance indicative of a different condition from that attending the other
groups. The great amount of finely levigated mud might, however, have rendered the ocean
too turbid for their existence; and it is very evident that in an ocean where free sulphuric -
acid existed, organic forms would soon be destroyed; and though other circumstances were
favorable, this alone would prevent their existence.
Shrinkage cracks. – These phenomena, which were illustrated under Medina sandstone,
appear in the upper division of this group. The more argillaceous strata at West-Mendon,
where the surfaces are exposed, present all the appearance of the clayey bed of a shallow
pond which has been dried by the sun, the whole surface being divided into irregular polygonal
figures. The cracks are filled with the succeeding deposition, which differs a little in charac-
ter, and the lower one having previously become partially indurated, very clearly marks the
cause. These appearances are less abundant in this district than farther east. The same
strata at Schoharie, and in the Helderberg, are strongly marked by these shrinkage cracks,
which, in the slabs used for flagging stones, are as clearly defined as in a recent clay bed.
134 - GEOLOGY OF THE FOURTH DISTRICT.
Minerals. – The principal mineral of this group in the Fourth District, is gypsum, of which
many thousand tons are annually used. Sulphate of strontian, the sulphurets of zinc and lead,
or galena and blende, with rhomb spar, occur in the higher division of the group. The gypsum
is the only one of importance, all the others occurring merely in small specimens fit for the
cabinet. -
Sulphuric acid. – This substance, which is usually regarded as a volcanic product, occurs
in this formation in numerous localities. The most productive, and the best known, is the
“Acid Spring,” in the southwest corner of Byron in Genesee county. This place was exa-
mined many years since by Prof. Eaton, and his account corresponds with its present condi-
tion. The place presents a low blackened mound of vegetable earth, charred by the acid, and
entirely destitute of vegetation. At the time of my examination, there was no water flowing
from it, though the soil a few inches below the surface is quite damp. The surface is com-
posed of vegetable matter intensely sour to the taste; this is underlaid by a clay or sandy
clay, also intensely sour. It presents this character for the distance of several rods around,
and during the driest part of the season, is always moist. Several large stumps of trees stand
upon this mound, the roots of which, and perhaps the trunks themselves, have furnished the
vegetable matter. I was informed, that in the early settlement of the country, a copious spring
of intensely sour water issued from the top of the mound ; that in digging about it for the
purpose of making it deeper, the whole was lost, and since that time it has only flowed in
the spring of the year. The water is considered a specific in many diseases, and is carefully
preserved, and even carried many miles to be used as medicine.” -
Several wells in the town of Bergen yield a slightly acidulated water, particularly in the
dry season of the year. One of these, belonging to Mr. Gifford, and which was mentioned in
the Annual Report of 1840, contains so much acid as to coagulate milk, and is unfit for culi-
nary purposes. Several other similar instances occur in this part of the county, where wells
are rendered useless by the presence of this acid. I was also informed of two other springs
of the same kind, which I did not visit. One of these, Dr. Beck has examined, and finds the
water a dilute sulphuric acid, and the earth of the Byron spring yields scarcely any other
product. -
Brine Springs, or Salines. – This formation, as before remarked, is the one which gives
origin to all the productive salines of the State. Thus far no valuable ones have been found
west of Cayuga lake, though borings have been made at different points. As was remarked
in a previous page, the hopper cavities are not found in any degree of perfection in the Fourth
District, though they are of frequent occurrence in imperfect forms; and if their perfection or
abundance be relied on as the indication of strength or quantity of brine, it may be inferred
that the springs of Onondaga are superior to any that will be found to the west of this point.
From what is already known, it is not impossible that in some favorable situation, springs
may be found which will repay the labor and expense of working. Still, while the brine of
*—
* Annual Report of 1840.
ONONDAGA SALT GROUP. 135
Onondaga county continues so copious, and of a quality so superior, there is little probability
of any thing being found of equal value in the Fourth District. -
The origin of these brine springs has been so fully discussed by Mr. Vanuxem and Dr.
Beck, that it is quite unnecessary here, to enter into a detail of the numerous facts and their
natural inference, which to a great degree are already before the public. The addition of
new facts may hereafter place the subject in another aspect, and since there are now many
arguments supported by facts, which apparently favor directly opposite hypothesis regarding
the origin of the brine, it seems desirable that more information should be collected before the
subject can be finally decided in the minds of all. The rocks of this group, particularly the
lower portions, are far less accessible than farther east, consequently the means are less for
ascertaining the nature and origin of these brines. It is quite evident, however, that the
source, whatever it may be, is less prolific in a westerly direction from Cayuga county than
in that county and Onondaga, which presents the greatest development of the group.
Were it not that the deep excavation at the outlet of Seneca and Cayuga lakes has removed
the upper portions of the group, and at the same time affords a means of escape for the sa-
line waters, we might expect to find brine springs of good strength in this place. The recent
borings at Montezuma demonstrate the existence of strong brines at that point, and the occur-
rence of brine springs on the east and west margins of the marsh, where circumstances seem
unfavorable, also offer facts favoring this view. -
The Galen salt spring in the town of Savannah formerly yielded a sufficient supply of
water for the manufacture of salt in the early settlement of the country, but the proportion
of saline matter was only about nine per cent. This spring is directly on the western edge
of the Cayuga marsh.
At Clyde, a deep boring was made for salt water, where no spring previously existed;
small quantities of strong brine were obtained, but the work was abandoned after penetrating
four hundred feet.” More recently a spring has been discovered a little east of the village,
and a boring to some depth has been made ; the water is sensibly salt to the taste, but it has
not been analyzed, having only come to notice when the survey was nearly completed. Salt
was formerly manufactured from a spring about two miles east of Lockville. These springs
are all in this group, and indicate a common origin with those farther east.
In Monroe county I am not aware of any brine springs in this formation, though several
are known in a lower rock. The only brine spring which I have seen in the Onondaga salt
group west of Wayne county is in the town of Elba in Genesee county, on the land of John
G. Satterlee. It is the most copious and strongly impregnated saline in the Fourth District.
The fact of its origin being in rocks of the same formation as those of Salina and Monte-
Zuma, renders it the more interesting. When I saw this spring the water was flowing from
one point in quantity about as much as a common pump would supply, and of a decidedly
saline taste. The vegetation is destroyed for several rods around the place, and there are
* See Report of Dr. Boyd, page 318, Annual Report of 1838.
136 GEOLOGY OF THE FOURTH DISTRICT.
indications of another spring coming into this from the west. In an adjoining field on the
east there is another spring, and several more in the vicinity. All these however are inferior
in strength to the first. The principal spring rises in a marsh, on the margin of which for-
merly were several wells, and from these salt was manufactured. .
The rock is eighteen feet below the surface, and the portions brought up in excavation and
boring are a grey marl, with nodules and seams of gypsum, being apparently the rock below
the lowest range of plaster beds. Several years since, a well was dug as far as the rock, and
a boring was made of fifty feet deeper. A wooden tube of two inches in diameter was then
placed in the opening, and the water immediately rose in it several inches above the surround-
ing surface, and flowed over the edge, keeping the tube constantly filled. At this period, and
for some time afterwards, a larger quantity of water flowed off than had risen in the well pre-
viously, and the vegetation for some distance was entirely destroyed; even small trees, for a
quarter of a mile along the course of its outlet, were so much affected as to destroy the leaves.
The situation of this spring, the copious supply of water, and the numerous smaller ones
around it, show a concentration of the saline matters which nowhere else appears in the Fourth
District. The quantity of water is greater, as well as stronger; and it is very probable, from
all the facts in the case, that it will eventually prove valuable as a saline for the salt manu-
facture. Since the supply of this article so essential to the wants of man, is one of interest
to the State, and since the salines of New-York are superior to any others in the country, it
is very desirable that a little attention be given to increasing and extending this source of State
wealth. * 2 :
Wells and Springs. – Along the southern borders of this formation, the water, which has
accumulated in the fissures of the limestone above, finds its outlet in springs which are copious
and abundant. This part of the formation is well watered; but in its middle and northern
extension, however, this group produces few springs or running streams, and the wells, unless
dug to great depth, fail in dry seasons. The strata are pervious to water, by the numerous
seams and fissures, particularly that portion containing gypsum beds, and the division next
below. Water is not readily obtained, unless by sinking to the level of the water courses of
the surrounding country. This often requires great depth of boring or excavation, and from
some of these we have derived much information of the character of the strata. Wide fis-
sures, evidently water-worn, are often met with in the excavations; and these have probably
resulted from the enlarging of the natural joints of the rock, by which the water first found
8,CC0SS,
Agricultural characters of the Onondaga salt group.
The belt of country occupied by this group in the north part of Seneca, and in Wayne
county, is mostly covered by a series of parallel hills and valleys. The hills consist of gravel or
a mixture of gravel and sand, and sometimes are entirely arenaceous; while the valleys are of
clay, with varying proportions of gravel and sand. Farther west this regularity ceases, though
as a general characteristic the surface is one of low hills and valleys, the latter presenting a
ONONDAGA SALT GROUP. 137
clayey soil, while the former consist of gravel or an admixture of clay and gravel. These
hills of gravel are often composed of rounded pebbles, with a large proportion of half-worn
fragments of the marls and shaly limestones of the Salt group; and where freshly exposed,
these are constantly crumbling from atmospheric agency. In the western part of Genesee,
and along the whole width of Erie county, the surface is more level, and the hills of gravel
are less prominent; still, however, it has some features in common with the surface farther
east. We find slight elevations of loamy or gravelly soil, covered with oaks; while the broad
flat clayey bottoms support maple and beech, with some evergreens.
The prevalence of what are termed “Oak Openings,” or tracts which are covered with oak
trees rather thinly scattered, but fresh and thrifty; and in other places, tracts of the same
timber in closer growth, with all the shrubs and smaller vegetation intermingled, indicates a
fertile soil, and one capable of yielding good crops of grain. Neither is the fact at variance
with the inference; for along this whole extent, there is rarely a better wheat-growing country
to be found.
Organic Remains of the Onondaga Salt Group.
From the nature of this formation, being one of finely levigated mud, with a large proportion
of saline ingredients, and even free acid, which is destructive to all organisms, and particularly
to the testacea, it might be inferred that few of these forms would be found. If they have
ever existed in any considerable numbers, they are no longer visible; but the stronger pro-
bability is that they have not existed at all, except in the few cases and the rare intervals which
have been observed.
Nearly all the forms seen in this group in the Fourth District, are presented in the accom-
panying woodcut; the shells almost entirely removed, casts only remaining. Since the group
is not identified by its fossils, these are chiefly interesting as presenting the continuation of
vital energy from the last group upwards. The specimens figured were all collected by Dr.
Boyd, in Wayne county. -
54.
|
º-
|
|
ſ
|
|
|
º
|
|
|
|
#.
|iº
º
yº \ º
|
|
ſ
ſ
|
|
|
|
º
1. Cormulites. 3. Loxonema Boydii. - 5. Delthyris.
2. Orthoceras lave. 4. Euomphalus sulcatus.
7. Avicula triquetra.
[GEOL. 4th DIST.] 18
6. Atrypa.
I38 GEOLOGY OF THE FOURTH DISTRICT.
1. Cornulites, n. S. – This species differs from the one in the Niagara group, in being
much smaller, quite straight, and the upper edges of the rings thinner. The upper edges of
the rings are not horizontal, but depressed on one side uniformly, producing a sort of seam or
Suture. -
Locality—Near Newark, Wayne county.
2. Orthoceras love, n. S. – Smooth ; annulations numerous ; very gradually tapering;
siphuncle central. - - * .
This is the only known Orthoceras of the group, and differs from any in this part of the
system, in its smooth shell, gradually tapering form, and numerous septae.
Locality—Newark, Wayne county.
3. Lowonema Boydii, n. s. –Very gradually tapering; last whorl somewhat ventricose,
slightly umbilicated; mouth imperfect. The marks of the arched or undulating striae, so
characteristic of the genus, are impressed upon the cast in a few places, and a little of the
shell is preserved. The summit of the spire is concealed in the matrix, and from its fragile
nature, it is impossible to remove it.
This shell is named in honor to the memory of Dr. G. W. Boyd, who was zealously en-
gaged in the New-York Survey during the first two years after its commencement; and after-
wards, until his death, in the Geological Survey of Virginia. -
Locality—Near Newark, Wayne county.
4, Euomphalus sulcatus, n. S.–Shell rapidly tapering; whorls about four, last one much
expanded; surface marked by spiral furrows and elevated lines of equal width, which con-
tinue into the umbilicus; aperture circular ; umbilicus large. -
The figures are from two different shells, the lower one representing the base being much
the larger. The lines and furrows of equal size readily distinguish this shell from any other
in this part of the system. It resembles the E. sculptus, (Silurian Researches, p. 626, pl.
12, f. 17,) in many respects, but is a smaller shell, and has four whorls.
Locality—Newark, Wayne county—abundant.
5. Delthyris — ?—This species is about the size of D. decemplicata of the Niagara
group, and since only casts have been seen it is left for further investigation.
6. Atrypa *—This species is apparently identical with a form abundant in the Nia-
gara shale, but which has not yet been identified or named. It is interesting as showing one
form of that group which continued beyond the middle period of the salt group.
Locality—Newark, Wayne county. '.
7. Avicula triquetra, n. S. — Shell obliquely subovate or cuneate ; marked with concentric
striae ; posterior wing large, abruptly acute; anterior wing very small.
Locality—Near Newark, Wayne county. The same apparently, appears in Genesee county
in the shaly limestone above the plaster beds. -
ONONDAGA SALT GROUP, 139
In addition to the fossils here enumerated, the Eurypterus lacustris of Harlan is said to
occur at Williamsville in Erie county. I have not been so fortunate as to meet with it,
though some fragments of a crustacean have been obtained from that locality.
Localities of superposition among the rocks of the Onondaga Salt Group, and the newt
- succeeding rocks.
All the sections here presented and other similar ones are constructed from a careful exa-
mination of the rocks, and none are given except where the actual junction of the two groups
is visible. In some instances much time has been spent in searching for the precise point of
contact, in order to ascertain whether the change from one rock to another was abrupt, or
whether it was by gradual intermixture of the superincumbent mass. The object in present-
ing them is to direct those who are examining these rocks to points where the contact of two
groups can be seen—always a point of interest to the geologist, for there he finds the termi-
nation of a condition of things which gave origin to peculiar forms of animal existence, but
few of which were continued beyond. -
--- --sºm-----
- *-* sm- -º-º-º:
-º-º-º-º- rººm-º.
& - - .
22* - • *
Section at Vienna, Ontario county.
d. Onondaga limestone.
c. Oriskany sandstone, with concretions, four feet.
b. Some thin dark layers of impure limestone, representing the Water-lime group—two feet.
a. Terminal mass of the Salt group-used for hydraulic cement.
Nearly the same order among the strata is to be seen a few miles west of this point.
The next section shows the order at Tinker's quarry in West-Mendon, Monroe county.
56.
s • *— & & <– « < < ~
€ Art T2-Z Z-2 fº *::::::== 2 <=
=–2—t-º-º-º-º-º-º-ººººººººººººººººººººº…E.T.:
_22–2–Z-Z-ZEZEzT- < <– 2 …—
24"– 2- £=——º Aº
Q. 2–3– e: 2–2 ºf 4-tº-2 24–º-
- % z -3 _* -z-z:E
*
~ º 2 < z=z <–27– 2 – 4–
sºmsºmº
c. Onondaga limestone, containing numerous coralline fossils, and embracing nodules of chert.
b. Coarse greenish sandstone or conglomerate, representing the Oriskany sandstone—four inches.
a. Upper part of Onondaga salt group, exhibiting about twenty-five feet in thin courses of a light ashen color, and entirely
destitute of fossils.
18*
140 . GEOLOGY OF THE FOURTH DISTRICT.
Section at Morganville, Genesee county.
1. Onondaga limestone, with fossils; in several courses,---------------------------------------------------- 3 feet.
* Oriskany sandstone, very distinct,----------------------------------------------------------------------- 4 in.
3. Hydraulic limestone in thin courses,--------------------------------------------------------------------- 4 feet.
4. Hydraulic limestone in thick strata—one being 6 to 8 feet thick—siliceous in character, and embracing numerous
irregular cavities, -------------------- - - - - - - - - - - - - - - - -* * * * * * * * * * * * * * - - - - - - - - - - - - - - - - - --------------- 22 “
5. Hydraulic limestone in thin grey layers, with seams of blue marl, ---------------------------------------- 12 tº
6, Bluish marl, crumbling into irregular, angular fragments, * * * * * * * * * * * * * * * * * * * * * * ºn tº us ºn tº tº se º as a we sº gº ºn s we as we as sº tº as we gº ºn as as se 5 *
7. Grey and greenish marl, with some portions very compact, 10 or 12 feet of the lower part filled with small cavi-
ties or pores like those in the rock covering the gypsum, .......------------------------ --------------- 19 “ .
This section not only presents the contact of the two groups, but exhibits the gradual
changes in the upper part of the salt group where it passes from its usual marly and shaly
character to the impure limestone which terminates the whole. *
At Black-Rock, the junction of the two groups is plainly visible, the salt group terminat-
ing with a drab limestone containing numerous irregular cavities, and succeeded by the On-
ondaga limestone, there being no representative of the Oriskany sandstone. -
About three miles east of Black-Rock there is a quarry where the junction of the two
groups is plainly visible. The limestone below the Onondaga is channelled or grooved into
trenches of six or eight inches deep, and as much in diameter, in which the latter appears
to have been deposited.
In the eastern part of the State there are several formations succeeding the Onondaga salt
group, which at the west are only meagrely developed, or are entirely wanting. Some of
these have apparently existed, and were swept off by denudation previous to the deposition
of the higher masses. Others have probably never extended far westward, one or two of
them scarcely appearing beyond Schoharie county, where those limestones forming the Hel-
derberg division are better developed than elsewhere in the State. sº
These rocks and groups will be enumerated in their proper order.
ū% : - -
!, 8.*, *... : , ...i.
§ ##$! --
º, ; , . . . .
* * * *
WATER-LIME GROUP. 141
WATER-LIME GROUP.
Water-lime Group of Manlius (Annual Reports). Water-lime rock 2 EATON. Tentaculite
limestone.
(PART of No. 6, PENNSYLVANIA SURVEy.)
The only locality in the Fourth District where the rocks of this group are known to con-
tain their characteristic fossils, is in the town of Phelps, Ontario county. Near Vienna vil-
lage, and at Maffit's quarry, about two miles northeast of this point, are some thin layers which
succeed the rock usually burned as water-lime, and which is the upper part of the salt group,
as before stated. These layers contain the fossils typical of the group. It is understood that
in the Third District these fossiliferous layers embrace the rock burned for hydraulic cement,
whence the name of the group. +
In Schoharie county, where these fossiliferous layers are well developed, they embrace no
hydraulic limestone, and the salt group lies immediately beneath them, the more compact
portion of which is known as the waterlime. - -
In the Annual Reports of the Fourth District the term water-lime has been applied to the
terminal mass of the last group, as being that rock from which hydraulic cement is prepared
in numerous localities, and possessing all the essential qualities of that substance. The rock,
therefore, known as the water-lime throughout the counties west of Cayuga lake is described
as the upper division of the salt group, and which according to the Report of the Third Dis-
trict does not correspond with the water-lime of that portion of the State, but with the mag-
nesian deposit of the Onondaga salt group.
These explanations seem necessary to a right understanding of the matter, since it is
desirable if possible to render a description of the rock under the name by which it is com-
monly known. - - - -
The strata identified by their fossils as the water-lime group consist of thin courses of
dark colored or bluish limestone, often not more than half an inch thick, and when struck by
the hammer emit a ringing sound. The characters are much the same as this rock presents
where it has been examined further east. The Favosites which are usually an accompaniment.
of this group when fully developed, do not appear here. - -
The thin layers when exposed to the atmosphere present numerous linear cavities, which
cross the surface in all directions and cause a destruction of the mass. When freshly ex-
posed or when a layer is split, the centre will be found presenting the same linear cavities
containing acicular crystals of sulphate of baryta. These, as the stone becomes exposed are
dissolved and the cavities left. The crystals and cavities cross the fossils as well as the other
parts of the stone separating them into numerous divisions.
142 - GEOLOGY OF THE FOURTH DISTRICT.
The illustration represents a small portion of the stone as it appears, one part presenting
the cavities while at the other extremity the crystals still remain. -
In some parts of the salt group, cavities of this kind abound, but I have never seen them
filled with any crystalline substance. These are probably due to a similar cause, viz. the
solution and removal of some crystalline matter by atmospheric agency. .
The fossils of this group (except No. 1,) occur at Maffit's quarry as before stated. They
are not however well preserved, though their forms are easily recognized. These are all
figured by Mr. Vanuxem in the Report of the Third District.
1. Orthis? (Delthyris) plicatus. 3. Tentaculites ornatus. - 5. Atrypa sulcata.
2. Avicula rugosa. 4. Littorina antiqua. 6. Cytherina alta.
Water lime, or Hydraulic cement.
The subject of water lime as a cement in situations exposed to moisture, or to alternations.
of wet and dry conditions, is one of the highest interest to the people of the State of New-
York. The great extent of our canals, where this substance is largely used in locks, aque-
ducts, culverts, etc., renders it desirable that the utmost precaution be taken to provide a
material which shall meet all the requisitions. Since, however, it is acknowledged that much
of the cement is of inferior quality, and as the subject is especially taken under the direction
of the engineers to guard against the use of improper materials, it is plain that there is room
for improvement in this product, either in the article selected, or in the manner of preparing it.
In order to produce a cement of the desired quality, the admixture of certain ingredients in
the proper proportions is required. The material selected and used sometimes produces this
WATER-LIME GROUP. - 143
desired quality, and sometimes it does not; but if the quality were always uniform, and the
treatment in preparing it the same, there would be as much certainty in the result as in the
burning of common quicklime. The evil, however, lies in the following circumstances. The
rocks used as hydraulic cement, along the Erie canal and the lateral canals, hold two distinct
positions, but both similar in regard to the nature of their ingredients. The lowest position
is the beds of passage from the shale of the Niagara group, to the limestone above. These
beds consist of shale, or argillaceous matter with an intermixture of arenaceous and calcareous
earths. The passage from the shale is gradual, the proportion of the other earths constantly
increasing: in the upper part the first is in small proportion, and the latter in excess. The
central beds are those best fitted for hydraulic cement, while the upper are too calcareous,
and the lower too argillaceous. -
In like manner, the second position of the water lime is at the passage of the argillaceous
marls and shales of the salt group to the more pure calcareous formations above; consequent-
ly there is a gradual diminution of shaly, and an increase of calcareous matter, with occasional
bands of pure shale. Now it is evident that the rock, taken indiscriminately, will produce a
lime of very variable quality, from the constantly varying composition of the rock. A single
stratum, indeed, at an interval of a few rods, may often be of a quality and composition very
different from the same at another : this may happen, too, without any very sensible difference
in the external appearance. It requires, therefore, the most constant attention in the selection
of the material, and a due degree of care in the preparation. There will always be, how-
ever, a tendency to excess of argillaceous matter in the cements as they are at present se-
lected; and this substance ensures their gradual but constant and certain destruction, to the
injury of the structure in which they are used. . . . . . "
The quality of the sand used in the preparation of the cement, is another subject of impor-
tance. In one part of the State, what is called sand, differs essentially from the material which
is known by the same name in another. In many places a pure siliceous sand is not to be
found, calcareous and argillaceous earths forming a considerable proportion. In other places,
the sand is purely or principally siliceous. The subject of cements has, however, been placed
before the public in the Annual Reports, and it would be unnecessary to go into further detail
in this place. The position which these substances occupy is indicated in the description,
and the places through which they pass is readily found by reference to the Geological Map. -
144 GEOLOGY OF THE FOURTH DISTRICT.
14, PENTAMERUs LIMESTONE.
(PART of No. 6, PENNSYLVANIA SURVEy.)
According to the Report of the Third District, this rock, being one of the subordinate
divisions of the Helderberg series, disappears from thinning out, in the vicinity of Oneida
creek. It is not recognized in the Fourth District as a distinct rock, though the charac-
teristic Pentamerus, or one very similar to it, has been found near Buffalo. This circumstance
with others, induces the belief that some of the lower rocks of this series appear farther west
but that they have not yet been distinctly recognized. The constant association of the Pen-
tamerus galeatus (Atrypa galeata, DALMAN, HISINGER ; MURCHISON, Silurean Researches,
p. 623, pl. 12, f. 4), with this rock gives the name by which it is known. It will not be con-
founded with the Pentamerus limestone, which is a subordinate member of the Clinton group,
the typical fossil of which is the Pentamerus Oblongus (see page 70). Another singular
fossil of this rock is the Lepocrinites Gebhardii."
15. DELTHYRIs SHALY LIMESTONE.
Catskill Shaly Limestone. Geol. Report of the Third District.
This rock is enumerated in the order of succession, though it does not occur in the Fourth
District.
As its name implies, it is a shaly mass, or consists of shaly with alternating beds of com-
pact limestone. Its present and former name is derived from the abundance of the Delthyris
macropleura of Conrad which everywhere marks the rock. The name of Catskill Shaly
Limestone, which has been proposed on account of its great development on the Catskill Creek,
is found to be objectionable, as it at once carries the mind to the Catskill Mountains, a very
different group of rocks, thus tending to propagate a false impression. Since the name now
used has been previously adopted, there can be no objection to continuing it.
It is an exceedingly interesting rock from the great number of species, abundance and
perfection of its fossils, many of which are very similar to those of the Niagara shale, and
of the Wenlock shale of England, some indeed appear to be identical with those of the latter
rock. Fossils appear in this rock very analogous to the following forms, which are figured in
* See Report of the Third District, page 117. Also the forthcoming Report of the Second District, under the head of
Pentamerus limestone. r - w
ENCRINAL LIMESTONE. 145
pl. 13 of the Silurean Researches. Orthis hybrida, O. canalis, Atrypa rotunda, A. linguifera
and several others. Spirifer? pisum (Silurean Researches, pl. 13, f. 9) is identical with a
fossil found in this rock.
This rock is the lowest position yet known where the remains of fishes have been found.
A specimen of the defensive fin bone (Ichthyodorulite) of some unknown species, more than
eight inches long and imperfect at both ends, has been found in this rock. Its greatest
breadth is about one inch, and a transverse section presents the form of two very acute tri-
angles with their bases in contact, forming the centre of the bone.
I have lately seen some fossils from near Point Abino in Canada, which appear referable to
forms found in this rock in the Third District, particularly the Atrypa lavis of Mr. Vanuxem.
Since this rock is not known to extend within the Fourth District, no illustration of its
numerous and beautiful fossils are given.
16. ENCRINAL LIMESTONE.
Scutella Limestone of the Annual Reports.
(PART of No. 6, PENNsylvania survey.)
This mass has no existence in the Fourth District, thinning out east of the central part of
the State, and appearing in force only in the region of Schoharie and the Helderberg.
It contains a great abundance of a flat or saucer-shaped pelvis of a crinoid, from the re-
semblance of which to the Scutella it received the name, Scutella limestone. Broken co-
lumns and other remains of Crinoidea, in a perfectly crystalline condition, are very abundant
in this rock.
17. UPPER PENTAMERUS LIMESTONE,
(PART of No. 6, PENNsyLVANIA SURVEy.) ... •
This mass succeeds the last, resting directly upon it. Mr. Gebhard junior, of Schoharie,
has clearly demonstrated that by its peculiar assemblage cf fossils it is distinguished from any
other rock. Among these, is a species of Pentamerus, in shape like P. Galeatus, but quite
smooth, and evidently a distinct species. Several forms of Atrypa also occur in this rock,
very similar to those below.
The thorough practical acquaintance of Mr. Gebhard with all the rocks of this part of the
system, and his nice discrimination of their fossil contents, renders his opinion decisive in
such distinctions.
GEOL. 4th DIST. 19
146 GEOLOGY OF THE FOURTH DISTRICT.
18. ORISKANY SANDSTONE."
(No. 7, of THE PENNSYLVANIA SURVEy.)
This rock, where best developed in the Fourth District, is a coarse, rather loosely ce-
mented, purely siliceous sandstone, of a yellowish white color. It contains some flattened
nodules of chert or flint, and cavities lined with the same mineral, approaching in appearance
to chalcedony. In the upper part of the rock are numerous concretions of dark-colored or
nearly black compact crystalline sandstone, very hard and tough. ' These vary in size from
an inch to five or six inches diameter; their external character is much like boulders of some
hard primary rock. - -
In other localities in the district this rock is scarcely recognizable. In Monroe county, its
only representative is a layer of greenish conglomerate about four inches thick. (See illus-
tration No. 56.) It is composed of coarse sand and small pebbles, with some fragments of
the light-colored argillaceous limestone derived from the next rock below. At one or two
other points it appears as a coarse sandstone of a few inches in thickness, resting on the Onon-
daga salt group. The last place in the district where it has been noticed is in the bed of
Black creek at Morganville in Genesee county.
The general absence in the district of the four last-named rocks, either from thinning out
or from subsequent denudation, forms an interesting subject of inquiry. The Oriskany sand-
stone seems to be deposited in depressions formed either from the natural inequalities in the
surface of the previous rocks, or arising from denudation. The presence of worn fragments
and pebbles of the argillaceous limestone of the salt group proves that denudation did take
place after the latter rock had in some degree become indurated.
Farther west where there is no representative of the Oriskany sandstone, the surface on
which the higher limestones rest is very uneven, consisting of abrupt elevations and depres-
sions very similar to the channelled bed of a powerful stream. There have, however, been
no grooves or striae observed; but since the appearances just noticed are usually seen in the
face of cliffs, or in the sides of quarries, it is by no means certain that such marks do not exist.
should this fact once be established, it will open a vast field, both for observation and spe-
culation. The absence of rocks, whether from thinning out, owing to want of material, or to
removal since deposition, involves some interesting points of inquiry.
In the present case, if the formations between the Water lime and the Oriskany sandstone,
which appear in the eastern part of the State, have never been deposited in the west, then the
* OrisKANy. The aboriginal name of this place is Areskana, signifying the residence of the God of war, and was a place
where the Agamousioni or United Braves held their war councils. - -
For this information my readers are indebted to Giles F. Yates, Esq. of Schenectada, who has given much attention to
the aboriginal names along the Mohawk valley.
ORISKANY SANDSTONE, $47
Water-lime, and more extensively the Onondaga salt group, must have remained, exposed
above the surface of the ocean, or forming its bed in situations beyond the reach of any de-
tritus or deposition. The production of these four rocks, Pentamerus limestone, Delthyris
shaly limestone, Encrinal, and Upper Pentamerus limestone, each marked by a distinct as-
semblage of fossils, must have required a long period of time; and we can scarcely conceive
of a condition of the ocean which would continue so long free from deposits of some kind,
even though at great depths or distance from land. Since the point of greatest development
of these rocks is less than two hundred miles from where they entirely disappear, it is im-
possible that if the Water-lime or Onondaga salt group formed the bed of the ocean, there
should not have been some deposition made upon its surface, and which has subsequently
been removed.
The evidence of shrinkage cracks in the upper part of the Salt group is a more prominent
character in the eastern part of the State, where the rocks in question are well developed, than
in the western part. Still in both places they exist, and are proof of the exposure of the sur-
face above water. If we are unwilling to admit of this denudation to a considerable degree,
we shall be forced to conclude that the Onondaga salt group was elevated above the ocean,
and formed dry land, while the eastern portion was yet depressed below its surface, allowing
the deposition of these limestones. -
Since also these formations are absent throughout the whole or a large portion of the wes.
tern States, the same cause which operated here has also operated over this great extent, and
we shall either admit a vast tract to have been elevated above the ocean, or that denudation
has operated over this wide area. -
From all that we know, however, there seems not the least probability that all these rocks
ever extended far westward; for there is a gradual diminution of the material, as appears
where the strata are exposed toward their westerly termination, and if the ocean covered all
the surface beyond, the deposit has been so slight that subsequent operations have removed
it. This seems the more probable conclusion, since we should expect to find evidence of the
fact, had so large a surface remained above the ocean during this period.
One of the most characteristic features of the Oriskany sandstone, is the abundance of small
cavities which have been formed by the destruction of fossils. These present themselves in
all cases where the rock is well developed. The porous nature of the mass has admitted the
percolation of water, which has dissolved the calcareous matter of the shells, usually leaving
casts of their internal structure. Where free from organic remains, it forms a fire stone of
approved quality. - '.
This sandstone is well known in Pennsylvania and Virginia, constituting an important for-
mation; and according to Prof. H. D. Rogers,” it is seven hundred feet thick in the former
State. In New-York its greatest thickness is not more than thirty feet, and usually much less.
j
y
* Geological Report, 1838, p. 51.
*
k
19*
148 GEOLOGY OF THE FOURTH DISTRICT.
It is not everywhere the purely siliceous sandstone which appears in the western part of
the State. At Schoharie and in the Helderberg generally, it is a siliceous limestone, very com-
pact and tough where penetrated beyond the influences of the weather; but very rough and
with numerous cavities upon the exposed surface. It received the name of Shell grit from
Prof. Eaton, from the abundance of its fossils and its siliceous character.
Organic remains of the Oriskany Sandstone.
The most obvious of the fossils of this rock are figured in the following woodcut from Mr.
Wanuxem’s Report :
2. Atrypa elongata, 3. Atrypa peculiaris.
1. Delthyris arenosa (CoNRAD, Geol. Report, 1839, p. 65.) Shell semi-oval, depressed
in front; extremities of the hinge line rounded ; surface marked by about sixteen or eighteen
flat ribs on each side the mesial fold, and four or five on the fold; ribs, particularly near the
margin of the shell, crossed by elevated undulating lamellae or lines of growth ; beak in-
curved ; area rather large.
2. Atrypa elongata (ConRAD, Geol. Report, 1839, p. 65.) Shell ovoid, crossed by nu-
merous sharp radii, which extend from the beak to the base and sides; lower valve gibbous
in the middle, with an elevated ridge extending from beak to base ; lateral margins often
straight. -
This is an exceedingly abundant fossil, the radii often becoming obsolete towards the beaks.
It is often less contracted at the base than the figure.
ORISKANY SANDSTONE, ‘. 149
3. Atrypa peculiaris (Annual Report of 1841, p. 56.) Lower valve flat, concave towards
the base with the margins elevated, the front extending into a linguiform projection; superior
valve convex, front margin folding over the edge of the lower, and joining by a few serrae or
teeth. - .
This shell is known by its peculiar projection in front, the strong depression in the lower
valve toward the margin, and the folding down of the edges of the upper valve.
The fossils here figured are perfect, the shell remaining entire. Casts of these, however,
are the more usual forms seen. In the following woodcut two of these casts are represented:
§ % s
à --~ iſ/ |2 Š
à. ######, \###$
㺠º
*º \sº
* %% |...}\!\|| § s §
% ñº"WW. §§7/,
% - § ſ §
- % \\ w § §
sº §§ sº º g º
in W
4. Cast of Atrypa unguiformis. 5. Cast of Delthyris arenosa.
4. Atrypa unguiformis, CONRAD. (Hipparionia proacimus, WANUXEM, Final Geol. Report,
p. 124, fig. 4.) This fossil, usually found as a cast, so much resembles the impression of a
horse's hoof, that it has for a long time maintained the name, and even by well-informed per-
sons it was considered as the impression of the hoof of some animal.
This is one of the common forms in the rock, and will be readily recognized.
5. Delthyris arenosa, ut supra. This is the usual appearance of the cast; it is distin-
guished by its projecting beak, which is often broken off much shorter than here represented.
In addition to the fossils here figured, there are numerous other forms which are almost
equally abundant. At Vienna, Ontario county, I obtained a species of Ichthyodorulite about
four inches long; the specimen however is too imperfect to represent in a figure. Several
others were seen in some blocks of stone from the same place, which were used in the glass
factory at Clyde. These however were partially dissolved by the percolation of water through
150 GEOLOGY OF THE FOURTH DISTRICT.
the porous sandy mass, and only a loose spongy substance remained. This is the second rock
in the ascending order in which remains of fishes have been found.
From the researches of Prºf. W. B. Rogers in Virginia, and Prof. H. D. Rogers in Penn-
sylvania, we learn that the Delthyris arenosa and Atrypa elongata are equally abundant in the
same rock, and one of the distinguishing features of the rock are the cavities resulting from
the removal of the calcareous matter of the shells. These facts show the wide distribution of
species over similar beds. It should be remembered also that these fossils so abundant in
this arenaceous deposit are often as numerous in almost purely calcareous beds forming the
termination of the mass. It seems very probable also that the original deposit was more cal-
careous, and that the porous character of the rock may have resulted from the solution and
removal of calcareous particles. - - -
The connexion of this rock with those above and below it, is represented in the sections ac-
companying the Onondaga salt group, which show its diminution and final disappearance in
a westerly direction. -
19. CAUDA-GALLI GRIT.
Cocktail Grit of DR. Eights.
This rock is an argillo-calcareous sandstone, passing into a greenish shale with thin lami-
nae of sandstone and sandy shale. -
A portion of this rock is characterised by the presence of a Fucoides or some analogous
vegetable form, which when seen in parts, as they frequently are, have a fancied plumose
appearance, whence, with the lithological character, the name of the rock is derived.
This rock is not known in the Fourth District, though it is well characterized in the middle
and eastern parts of New-York and also in New J ersey, as we learn from the Report of Prof.
Rogers. -
SCHOHARIE GRIT, 151
tº . 20. SCHOHARIE GRIT.
Grit Slate of EATON.
This rock is a very fine-grained siliceous limestone or calcareous sandstone; when wea-
thered, the calcareous matter disappears, leaving a porous siliceous mass of a brownish color,
from the presence of hydrate of iron. In this condition it presents numerous casts of its
peculiar fossils. It abounds in a species of Pleurorhyncus, Orthoceras and numerous forms of
corals. The rock is well developed at Schoharie and in the Helderberg, but does not extend
far westward. It is unknown in the Fourth District, but with the last and several others it
has been enumerated in the order, that the numbering might be continuous, and a complete
series of the rocks of the system be given in their order of succession, believing that such a
course would facilitate the comparison of the groups in different parts of the State. There
are formations at either extremity of the State which do not exist or are only partially deve-
loped at the other, and if the practice of describing these in their respective order in the
report of each District be followed, neither would present a complete series of the rocks of
the system. This course will give the inhabitants of the western part of New-York a know-
ledge of what exists elsewhere and which are wanting in that region, and also show them
the points at which they are introduced in the middle and eastern parts of the State.
21. ONONDAGA LIMESTONE.
Included in the Corniferous Limerock, by Prof. EATON. Grey Sparry Limestone of the
Annual Reports. -
Throughout the greater part of the Fourth District the impure limestone terminating the
Onondaga salt group is succeeded by the Onondaga limestone with usually the intervention
of a few inches of sandstone before noticed, which in ordinary observations might be entirely
overlooked. There is also sometimes a thin band of nonfossiliferous bluish grey limestone.
The range of this formation is in an undulating line having a general east and west direction
throughout the district, extending eastward to the Hudson river and westward far beyond the
Niagara into Canada. Its northern outline is everywhere well marked, forming together
with the next succeeding rock the second great limestone terrace, which rises to the south of
the valley marking the range of the Onondaga salt group.
#52 GEOLOGY OF THE FOURTH DISTRICT.
By reference to the geological map accompanying the Reports, the course of this rock will
be readily traced through the District from Cayuga lake to the Niagara river, being indicated
by the blue band following the ochre color. The great depression southward in the line of
Outcrop at Cayuga lake, the Genesee and Niagara rivers indicate the great amount of denu-
dation it has suffered at these points which are the ranges of ancient valleys, formed at the
same period in which nearly all the large lake valleys and river channels of western New-
York were produced. The same cause and, in some places, more recent operations have
produced minor indentations in the outline, many of which are too small to be noticed in
the map. -
This rock is subordinate in thickness and continuation to the next succeeding mass, and
was not separated from that by Prof. Eaton. Indeed for all practical purposes they may be
regarded as one formation; the lower part, where fully developed, being marked by an as-
semblage of fossils which sufficiently distinguish it. *
Its usual characters in the Fourth District are a light grey color often approaching to white,
more or less crystalline in structure, and containing numerous fossils. In many instances
this mass, like the encrinal limestone at Lockport, seems almost entirely composed of broken
and comminuted fragments of crinoidea and corals, sometimes extremely attenuated, and at
other times fragments of large size are preserved. These fragments of crinoidal columns,
with some of the other fossils, are frequently of a pink or reddish color, and give a beautiful
variegated appearance to the mass, particularly when polished. The more comminuted por-
tions containing some earthy matter of a dark color, frequently embrace large fragments of
Favosites, a perfect Cyathophyllum, or some other fossil of a light color, which forms an
agreeable contrast with the surrounding mass. This character may be seen in the stone of
which the Court House at Batavia is constructed, and which is from the town of Le Roy.
Sometimes the mass is fine grained, more compact in texture, and of a darker color; when
it has this character, few fossil remains are detected in it. The layers are usually separated
by thin seams of greenish shale, which often divide blocks of the stone into wedge-form and
irregular laminae. These seams, barely colored with the greenish deposit, often exist in the
stone, where they are scarcely visible, though a blow with the hammer separates the block.
In selecting specimens where much vertical depth is required, this is frequently a great in-
convenience. -
Where thinly laminated by these seams of shale, and the surface covered with encrinital
columns and plates as it usually is, the rock bears a most striking resemblance to the Wen-
lock limestone of England, as seen in some specimens from Wenlock which were presented
to me by Mr. Lyell. So complete is the resemblance in some instances, that one might al-
most be mistaken for the other. Judging, however, from the general character of specimens,
and the description of Mr. Murchison, there is a greater amount of shaly matter intermixed
with the Wenlock limestone, than with our rocks of the same period.
The similarity or even identity of specimens from Dudley in England with those from the
Niagara group has been remarked; and if this inference be correct, of which there seems no
doubt, then we find a wide separation here between rocks which in England constitute one
ONONDAGA LIMESTONE, 153
group. That such is the fact however appears plain, for there are many fossils of the lime-
stones above the salt group, which are identical with the Wenlock formation, while the iden-
tity of so many species in the Niagara group leaves no doubt of perfect correspondence. We
are therefore to look upon the salt group as a formation, on this continent, coming in at a pe-
riod during which, in England, the rocks are supposed to belong to a continuous group, or to
be parts of one formation. -
The Onondaga limestone in many places contains nodules, or thin interrupted layers of
chert or hornstone (usually called flint); and sometimes the Favosites are partially dissolved
and the cavities lined with silex in the form of chert, chalcedony or crystals of quartz. The
alimentary canal of the crinoidal columns is frequently lined with crystals of quartz, and the
chambers of Orthocera, as well as the cavities of other shells, often present the same appear-
ances.
Its characteristic features, when well developed, and which are always much more prominent
than the lithological or mineral characters, are the presence of Cyathophylli, Favosites, and
fragments of crinoidal columns. These always accompany it in situations where it is suff-
ciently developed to be of much importance either in economical consideration or geological
interest. -
In Seneca county this rock is scarcely visible, or forms only a very subordinate layer and
destitute of its characteristic fossils. In the adjoining county it becomes of more importance,
first appearing as a thin layer near Oakes’ corners, and along the terrace to East-Vienna; at
the latter place it appears in the bed of the creek resting directly on the Oriskany sandstone,
and succeeded by the cherty layers of the corniferous limestone. It is but a thin mass at
this place, being little over two feet thick. At another point southeast of this the Onondaga
limestone is entirely absent.
At Wayland's quarry, northwest of Vienna, this limestone appears in several strata following
the water-lime, and marked by its characteristic fossils. A short distance to the southwest
of this quarry it appears again, containing Favosites and other fossils. The rock at all these
places is compact, of a greyish blue color and less marked by seams of shale than in many
other places.
At Manchester and in the bed of Mud creek at Freedon it is but slightly developed, being
a thin layer of a greyish blue color and destitute of fossils. It retains the same character as
far as Mendon in Monroe county, where it is better developed and contains a larger number of
corals and Cyathophylli. It has also the same character, or is even more fully developed, in
the town of Rush, where it disappears before reaching the Genesee river.
On the west side of the Genesee, it appears at Caledonia, still a thick compact mass, with
a few thin layers separated by shale, and containing a great number of Cyathophylli, Favo-
sites, and other fossils. For some distance north and west of this place, it maintains the same
character, and the surface is strewed with fragments which contain its typical fossils.
North of Le Roy village, on Allen's creek, the rock resting on the Onondaga salt group is
a compact sub-crystalline greyish blue limestone, containing no fossils; this is succeeded by
[GEOL. 4th DIST.] 20
154 GEOLOGY OF THE FOURTH DISTRICT.
twenty feet or more of chert in thin irregular layers, with scarcely any calcareous matter.
This cherty mass contains the usual fossils of the Onondaga limestone, and they are persistent
as far as the hornstone continues. The cherty layers are again succeeded by thin-bedded
compact, bluish or greyish blue limestone, marked by fossils typical of the next higher rock.
This example furnishes an instance where the fossils of the lower limestone pass into the
hornstone, which eminently characterizes the next rock, and from which its name is taken.
Should such cases prove to be of frequent occurrence, it might become a source of difficulty
in identifying these rocks. The fact is stated as occurring, not for the purpose of throwing
difficulty or obscurity in the way of the observer, but to prepare him for some variations in
character, which will ever be found in all subdivisions which can be made; and if he be not
previously made acquainted with them, he is likely to experience more difficulty in endeavor-
ing to force rocks to accord with arbitrary descriptions, than from a knowledge of any such
variations from the general rule.
About two miles northeast of the point just described, the cherty mass has greatly dimi-
nished, and the Onondaga limestone in its typical characters is presented in several thick-
bedded regular strata. It is of a light grey, often approaching white, composed of comminuted
fossils, and marked by the presence of large numbers of crinoidal columns, Cyathophylli and
Favosites. The crinoidal portions are often reddish or pink, and give a beautiful variegated
appearance to the rock. The quarries at this place belong to Messrs. Clifford and Rich.
Half a mile farther west, there is another similar quarry. The rock is extensively wrought,
sawed into slabs, and polished for hearthstones, mantels and other purposes. It is also much
used for buildings. From these quarries the stone for the Court House at Batavia was ob-
itained. There is scarcely a better locality in the district for an exhibition of the typical
features of the rock. | -
Following the outline of the terrace westward, this rock appears in several points, though
but obscurely developed, sometimes being represented by a single stratum of less than two
feet in thickness. In the town of Newstead, Erie county, its place is marked by a thin band,
almost entirely composed of Favosites and other corals, with a few calcareous laminae, and
a large proportion of shaly matter. The latter is partially decomposed, and the coralline
masses appear as if imbedded in a ferruginous mud.
At Clarence Hollow this limestone is but meagrely developed, a thin stratum resting on
the terminating rock of the salt group, being all that is seen. A mile west of this point, how-
ever, it is well developed, appearing as a grey sub-crystalline rock, very coarse grained, and
crumbling under a blow of the hammer. At this place it abounds in its typical fossils, and
in some places the mass is nearly composed of crinoidal columns and Cyathophylli. From
this place to some distance west of Williamsville, it continues to be a well-marked and highly
important rock. In some points it contains large numbers of silicified corals, and some irre-
gular nodules of hornstone, which render it unfit for lime burning. Every point, however,
where free from these substances, and the grey crinoidal mass well developed, is marked by
one or more limekilns, and it will be found a convenient guide to this rock throughout Erie
county to inquire for these. * * *
ONONDAGA. LIMESTONE, 155.
The best locality for examination of this rock is on the farm of Mr. Youngs, in the town
of Amherst, a mile west of Williamsville. At this place the rock is well exposed in all its
varieties. Being a point from which large quantities of lime are taken to supply the city of
Buffalo, the rock has been quarried at several places, much increasing the facilities for ob-
servation. The grey crinoidal mass is much better developed here than I have elsewhere
seen it, the masses of coral are larger and more numerous, and finer specimens can be ob-
tained. On the brow of the hill it is succeeded by the next rock, which however appears to
contain little hornstone.
From the point just noticed, the rock diminishes westward, and at Black-Rock there is but
a thin stratum marking its place. At the same time the chert or hornstone of the next rock
increases, and Cyathophylli and a few masses of Favosite have been found in the strata com-
posed in a great measure of this material.
From the facts mentioned, the inquiry naturally suggests itself, as to the conditions under
which this rock was deposited. It has already been seen that at some points it attains consi-
derable thickness, very remarkable for the abundance of its fossil contents, as well as the
character of the rock, while at others it forms a thin stratum scarcely distinguishable except
by its position. The materials of the formation therefore have either been very unequally
distributed over the bed of the ocean, lodging in depressions of the previous surface, or these
greater developments are only local, the materials being derived from the growth of coral and
other organisms in or near the situation they now occupy. Although the former cause may
have operated to some degree in many localities, it will not account for the phenomena wit-
nessed in all. The thin strata forming connecting links between the points of greater develop-
ment are probably the finer portions of the thick strata which were transported by the water
and spread over the bottom, where few or no organic forms existed. In this respect, these
thick portions resemble a line of detached coral reefs, which we may fancy to have skirted the
margin of this ancient ocean, and like many modern ones they may have flourished for a long
period entirely disconnected, and with a deeper ocean between them. That these deposits
are local, or have for the most part been produced in their present situation, seems proven
from the abundance of coralline forms, many of which retain the position in which they ori-
ginally grew. Some of the masses of Favosite are several feet in extent, and from one mass
several wagon loads were taken on the supposition that it was gypsum. It is plain that such
as these could never have been transported far, even if they have been moved at all. It is
true that many of the smaller ones are broken up, and others are found turned upon one side,
or completely reversed, showing the action of waves. The Crinoidea which appear to have
formed a large share of the deposit, are broken up and their remains scattered, though columns
of a foot or more in length sometimes occur. The Cyathophylli are generally thrown down,
though they are usually perfect. . - .
From the fragile nature of the Crinoidea, any force sufficient to overturn the broad-based
Favosites and other similar corals would destroy these, and scatter their fragments over the
bottom, filling up the spaces between the other corals. Many other small or fragile corals,
20*
156 GEOLOGY OF THE FOURTH DISTRICT.
as well as Crinoidea also existed, but of all these we only find fragments, which bear evi.
dence of being broken and worn previous to imbedding. In these situations fossil shells are
few, and it is only when the mass is more evenly distributed that they increase in number.
Now all these circumstances seem plainly to indicate that at these points of thickening
there was a part of the ocean bed, on which these corals had established themselves, and on
which they continued to construct their habitations for a long period, as the great size of many
would prove. In the more sheltered portions smaller and more delicate forms, with the Cri-
noidea seem to have flourished; the latter in great perfection, judging from the size of the
columns. The more exposed portions and the more fragile kinds were broken down as they
came within the influence of the waves, and these materials were spread around the base,
the coral reef extending in every direction as far as the material was transported, and
there we now find the mass thinning out. There seems in this nothing more than we might
expect, and probably only what is now accomplished in coral reefs which are near the surface
of the ocean, and which may be alternately elevated above or depressed beneath it. The
great amount of destruction here visible was not all accomplished at once, for we may find àI.
overturned mass of coral covered with a fine deposit, and upon this another mass of coral,
either overturned or in its natural position, the whole indicating a long continuation of the
causes in operation. The simple fact of the succesive growths of coral upon deposits cover-
ing other corals, of itself proves a great lapse of time; for the growth of all these forms is
exceedingly slow. f
From the amount of exposure, it is impossible to ascertain whether these coral reefs were
circular, or whether they formed more than a single line skirting the margin of the ocean.
From the great amount of denudation on the north, and the east and west extent of these coral
banks, we may infer that there was more than a single range; and if it can be proved that.
they existed far south of the present outcrop, we may rationally infer that they formed a series
of circular reefs, probably much in the same manner that similar reefs and islands are formed
in the present ocean. - -
The Onondaga limestone is scarcely anywhere developed in the same perfection as in the
First and Third Districts, where it contains a greater number of fossils, and as a distinct mass
is more persistent. As a quarry stone for building and other purposes, it rarely appears in
the perfection which it assumes at Syracuse, Le Roy being the only known locality where
this character is possessed in an equal degree; while in most other places where it is suffi-
ciently compact for that purpose, the strata are very thin.
Localities.—The examination of a few points in the district, will suffice to acquire an ac-
quaintance with this rock. The first locality of interest is at Vienna, where its connexion
with the rocks above and below are clearly seen. Two miles northwest of the same point, it
is better developed, and contains its peculiar fossils. Caledonia offers the next point of much.
interest, though the towns of Rush and Mendon, on the east side of the Genesee, are inte- -
resting in some degree. Le Roy, at the quarries before alluded to, offers the best exhibition
of this rock in the district. In Clarence there is also a good exposure, a mile west of the
ONONDAGA. LIMESTONE, - 157
village of Clarence Hollow. Near Williamsville, on the farm of Mr. Youngs, a large number
of the corals and other fossils of the rock may be obtained; and this locality, with Clarence
and Le Roy, are by far the best in the district. -
Thickness. – The thickness of this mass is very variable, being from one foot to twenty or
even forty feet. At Black Rock, the stratum representing this rock is fourteen inches thick;
in Newstead, Erie county, about the same; at Vienna, two feet. At Williamsville, as nearly
as can be ascertained, it is twenty feet. This point and Le Roy, where the thickness was not
ascertained, present the greatest development. -
Mineral contents. – The only minerals noticed in this rock, are crystallized carbonate of
lime, quartz in crystals lining cavities, chalcedony and hornstone, with iron pyrites in a few
places. The Favosites are often silicified, and their cavities lined with small crystals of quartz.
This rock is so intimately connected with the next in succession, and forms surfaces of so
little extent, that its characters in agricultural respects can scarcely be considered, but will
be noticed in connexion with the rock next in order. ,
} w
Organic Remains of the Onondaga Limestone.
The organic forms of this rock are its most prominent marks, wherever the mass is well
developed. In the Fourth District, Corals and Crinoidea were the predominating forms, the
conditions under which it was deposited being apparently unfavorable to the existence of
Testacea. A few univalve shells have sometimes been found, and more rarely some species
of Atrypa and Delthyris.
Among the numerous forms of corals, those of the three following illustrations have been
selected, as being the most common or most obvious among them. The number may be
quadrupled, without exhausting the species of this rock.
#
à
#
à
*
É
l
*:
#
#
.
:
:
:
:
i
#
i
|
#
s
i
i#
i
t:
#
|
Éi
r:#
3.
:
$:
>
:
§
i
i
#
É
É
§
:
§
*
#
tă
i
º-3.
:;i.
;i
i:-
-:w
:::::::::::::
# 3 d/ Aggiº
É # # ##$ º
- ää # wº
######## y
à
º
1 and 1 a. Favosites alveolaris. 3, 3 a and 3 b. Fragments of column and joints of
2, 2 a and 2 b. F. Gothlandica, unknown Crinoidea.
158 GEOLOGY OF THE FOURTH DISTRICT,
1. Favosites alveolaris.” This specimen has a honeycomb structure; the transverse septa
are interrupted. There are no pores visible, but from its analogy to others which are evi-
dently of this species, there remains no doubt of identity.
1 a. A specimen with larger columns, presenting the pores upon the angles.
Localities—Williamsville, Erie county; Le Roy, Genesee county; and Caledonia, Living-
St0m county.
2. Favosites Gothlandica. — A mass of solid columns, showing the pores upon the sides of
the tubes. * •
2 a. A single tube magnified twice, and presenting a double row of pores upon the side.
2 b. A fragment from a honeycomb specimen, showing the transverse lamellae.
Specimens from the mass from which these are figured, present the characters noticed by
Mr. Lonsdale, of having a single and a double row of pores upon the same specimen, and
upon the same column. ,- -
This is an exceedingly abundant coral, sometimes appearing with its tubes filled with cal-
careous matter as in fig. 2; and again with the cells in their original condition, presenting the
appearance of honeycomb, by which name this and some other species are known. It is
known to range from the Niagara to the Hamilton group inclusive, occurring in great perfec-
tion in nearly every rock. -
Locality of specimen figured—Williamsville, Erie county. Found in the same rock at
Caledonia, Le Roy, and numerous other places,
3. Fragment of a crinoidal column.—This is an abundant and characteristic fossil of this
rock. Its great size and general smoothness, with the very thin plates of which it is com-
posed, are sufficient to distinguish it. ' ' ,
3 a, shows the crenulated edges of the plates.
3 b, presents an appearance common on the surface of weathered slabs of this rock, where
the column has been broken down, and the plates have slidden over each other, still remaining
in contact. -
This form seems referable to fig. 9, pl. 18, Silurian Researches. Fragments of these co-
lumns a foot or more in length are sometimes found, and there are others where the columns
are composed of alternating larger and smaller plates.
Locality of specimens figured—Williamsville, Erie county. Found also at Caledonia, Le
Roy and numerous other places. -
- *
7
****
* For synonymes and references of the genus Favosites, see Silurian Researches, pp. 681, 682 and 683; also GoldFuss,
Petrefacta, Genus Calamopora,
ONONDAGA LIMESTONE, 159
62;
}%. 3. Nº
w * ºr - - # *:
Nºvi wº - %)
\}} ğ.
! NY'ſſ. %ft
§ Nº|| º
a \\\\||
º - º:
§§
§§
§§
Nº. 4/º
Nº. ſº
Wººyºº.º. -
§%
º % % =
§4%2: "º
º
W
§§ tº sººtu
º
§
- §§
§
ğ%
S
W
1 and 1 a. Favosites fibrosa,
1. Favosites fibrosa (Calamopora fibrosa, GoLDFUss, Petrefacta, pp. 82, 215, pl.xxviii,
fig. 3 and 4, and pl. lxiv, fig. 9. Silurian Researches, p. 683, pl. 15 bis, fig. 6, 6 a to 6f).
The figure represents a specimen of the natural size, being a portion of the whole, showing
the manner of its bifurcations. 1 a, is a portion magnified, but the transverse lamellae are not
visible. . . . "
This fossil is abundant in many places upon the surface of the strata. It seems referable
to this species of Goldfuss, though I have not been able to detect the connecting foramina;
there are also some other varieties which I have no opportunity of examining. This species
or a very similar one ranges from the Clinton group to the Hamilton. -
Locality—Clarence, Erie county.
2. Astrea rugosa, n. s. The surface of this fossil consists of a series of circular or inter-
rupted stars of about 3 of an inch in diameter, having an elevated disk in the centre of each,
which is composed of 18 rays; these rays bifurcate on the outer margin of the disk, and
form the 36 rays which compose the star. The rays are wrinkled, or crossed by concentric
lamellae, giving the surface a peculiar roughness, from which the name is derived; it differs
from any of Goldfuss' figures in the number and character of the rays.
Locality—Le Roy, Genesee county.
160 GEOLOGY OF THE FOURTH DISTRICT.
63.
§
-º
#\t|§
-º
}s§
:
ſº-º i
§§
§º
º
**
i
;
|
|
}
-;
--:º\
:|§º
º º
\\
\\
§
º
º
;
*** * *
W * §§
º:
º
1. Cyathophyllum. 2. Cyathophyllum dianthus. 3. Syringopora.
1. Cyathophyllum? It is impossible to pronounce with certainty whether this be a Cya-
thophyllum or Strombodes, as I have had no opportunity of examining its internal structure.
It is one among the common and abundant forms of the Onondaga limestone occurring with
C. flexuosum and C. ceratites. - -
2. Cyathophyllum dianthus. (GoLDFUss, Petref. p. 54, pl.xv, fig. 13, and pl. xvi, fig, 1.
Silurian Researches, p. 690, pl. 16, f. 12, 12 a to 12 e.) This coral usually appears in large
groups, which, from their silicified condition, stand out in relief on the surface of the rock.
The figure is a small portion from a mass of this kind, of the natural size.
Localities—Caledonia, Livingston county, Williamsville, Le Roy, &c.
3. Syringopora. This fossil often appears as in the specimen standing out in relief upon
the surface; at other times the ends of the coral are seen projecting, showing their structure
in the most perfect manner.
There are also two or three other species which are abundant in this rock. The one
figured apparently differs from any species of Goldfuss. -
The characteristic fossils of the Onondaga limestone in the Third District, figured by Mr.
Wanuxem on page 132 of his Report, cannot be considered as typical of this rock in the
Fourth District. The Pentamerus elongatus occurs at Vienna, but I have not seen it else-
where in the district.
CORNIFEROUS LIMESTONE. 161
F-: - ---
Eº-º-º-erº:
Sºº-Hºº-ºº: SElº.
22. CORNIFEROUS LIMESTONE.
Upper part of the Cornifero's Limerock of EATON. Seneca Limestone of the Annual
Reports.
This rock is one of the most persistent of any in the series, and at the same time maintains
a uniformity in lithological character, and in the occurrence of certain fossils, scarcely possessed
by any other. It is known to extend from the Helderberg mountains on the Hudson river,
to the Niagara river, and thence far into Canada. This rock forms the terminating mass of
the second limestone terrace to the south of lake Ontario, and with the Onondaga limestone
and the upper part of the Salt group forms the whole height of the same in the Fourth Dis-
trict. It follows the same line of direction as noticed in the last described rock, and every
where succeeds that mass, being always thicker and more prominent. By reference to the
Geological Map, the limits of this and the next lower rock will be seen, occupying in the
Fourth District a width of from two to four or five miles, dipping gradually to the south, and
disappearing beneath the Marcellus Shale.
It has suffered a great amount of denudation at several points, as noticed under the pre-
ceding rock, the two being almost always in the same line of outcrop.
This rock has a prominent and well defined outline upon the north, and gives rise to a
prominent feature in the topography of the country as well as to many interesting points in
the scenery. All the smaller streams passing over it present rapids or cascades of more or
less interest. The larger streams, and the lakes of Cayuga and Seneca which extend north
beyond this rock, have excavated their channels deeply into it giving no evidence of its exis-
tence in their beds. It forms a slight barrier however at the outlet of lake Erie at Black
Rock, producing a rapid current with considerable descent, and presenting a small island
just above the water which is all that now remains to show that the rock was once continuous
from the two shores.
[GEOL. 4th DIST.] 21
162 - GEOLOGY OF THE FOURTH DISTRICT.
Under the corniferous limerock of Prof. Eaton were included this rock and the Onondaga
limestone of the Reports, the latter constituting his “Ceratial rock,” so named from the abun-
dance of Cyathophylli which it contains. The name corniferous is continued as being pecu-
liarly applicable to this rock, though the other limestones contain the same mineral. This
is the highest limestone of importance in the series, which continues throughout the district.
In lithological character this rock varies to a considerable degree in its range through the
district, being at the eastern extremity a fine grained, compact limestone, scarcely presenting
any crystalline grains. Its color varies from a light greyish blue, to dark blue or black, and
it is sometimes even of a light grey or drab color. It contains numerous nodules of hornstone,
and the strata are sometimes separated by irregular layers of the same. In other localities
these layers of hornstone increase in number and thickness to the almost entire exclusion of
calcareous matter, and they then present a very harsh outline. Where it possesses this
character, the calcareous matter is soon dissolved out from weathering, leaving the hornstone
in jagged and irregular projecting points, from which it receives the local name of “chawed
rock.” In the central part of the district the hornstone portions are largely developed, and the
terminating mass in such situations is a light grey limestone, eften of a sub-crystalline texture.
At the eastern end of the district the hornstone is intermingled and interstratified with the
calcareous strata, the whole very dark colored. The same character prevails at the western
extremity of the district, where the rock outcropping on the Niagara has, from its black
color, given name to the village of Black Rock. -
The rock for the greater part seems to have been composed of finely levigated calcareous
mud, probably derived from the destruction of corals at distinct points, while at the same
time siliceous matter often formed no inferior part in its production. The characters which
distinguish the last rock, viz., the presence of corals and crinoidea are rare in this, and form
no essential feature. Fossils are generally few, and for the most part consist of shells.
Some portions it is true, though of small extent, appear as if they may have resulted from
the destruction of corals. -
This rock is usually distinguished from the limestone below, by its more compact structure,
the presence of hornstone in layers or nodules, and the absence of Favosites, and crinoidal
columns, which as before stated always mark the Onondaga limestone where well developed.
Where free from hornstone this rock furnishes a good building stone, and is readily dressed
to a smooth face. The darker portions however give a sombre aspect to the structures, and
the effect upon the eye and the mind is unfavorable. The lighter colored portions, usually of
the upper part are more suitable for such purposes, and give a good appearance to buildings.
That portion with much hornstone is only fit for rough walls, for if dressed smoothly, which
is difficult, it weathers unequally and the moisture finds its way between the nodules of horn-
stone and the surrounding mass, and eventually produces mischief. The upper part of the
mass is in many places so free from hornstone that it is extensively used for lime burning.
This rock is interesting to the geologist by its contrast with the preceding, both in color,
general lithological character and organic contents. It reveals a period when a great change
CORNIFEROUS LIMESTONE. 163
took place in the condition of the ocean, when from a sea teeming with organic forms like the
corals and crinoidea, it became one in which few of these forms existed, and shells almost
alone tenanted the deep. It appears to have been the commencement of a change by which
the sea grew deeper, finally to the depth beyond which corals flourish, and these were all
covered by the calcareous mud derived from previously existing masses. -
This rock first appears in the district in the eastern part of Seneca county, having the same
characters as in the quarries near Springport on the eastern side of Cayuga lake. The rock
is exposed at numerous points, nearly all presenting the same characters; being in regular
courses of from six to eighteen inches thick, usually separated by layers of hornstone, and
sometimes embracing flattened nodules of the same, which have a striated surface, as if from
the crystallization of some mineral in the space between the two rocks. A mile or two west of
Waterloo it approaches the Seneca outlet, and is quarried on the margin of the stream; some
of the upper strata are of a greyish blue color, weathering to a lightgrey or ashen, and con-
taining some argillaceous matter. These strata are often marked by the presence of a Cyr-
toceras, which often attains a large size. The greater part of the rock is fine grained, bluish
in color, embracing an irregular strata of hornstone. In one quarry I noticed a separation of
the higher and lower strata by a “wayboard,” or seam of clay about four inches thick.
This clay is exceedingly fine like the softest talc, and has a laminated structure and yel-
lowish color; it differs greatly from the usual shaly matter separating the strata, and on this
account is noticed. The rock at these quarries is readily worked, being crossed by vertical
joints in two directions, which often separate the stone into blocks of convenient size, and
leave a good back wall to the quarry. - -
The effect of these joints, and the manner of working the rock where they occur, is well
illustrated in the view of a quarry south of Waterloo, which stands at the head of the section.
The salient and reëntering angles, the lines of which bound the quarry, mark the two direc-
tions of these joints, one of which is nearly E. and W., and the other varying from N. 10° E.
and S. 100 W. to N.E. and S.W.
About three miles south of Seneca-Falls village it comes to the surface in several places,
and from always presenting the same strata above ground it appears to have been undermined,
or from some other cause to have been broken into faults. The surface being level does not
admit of an actual inspection of the condition of the rock, but judging from what is seen it
holds the following position.
65.
- º ji -
WW)sº.”: * *k, waſ fa, ºl.
• T, as * * * *.
This dislocation of the strata is probably caused by the removal of the soft gypseous rocks
from beneath, allowing the higher strata to fall down. From that side next to Cayuga lake
21*
164 GEOLOGY OF THE FOURTH DISTRICT.
only presenting this appearance, it is probably due in some measure to the cause which ex-
cavated the lake, and which doubtless acted with greater effect upon the softer strata beneath
the limestone. Upon the eastern shore of Cayuga lake, in the Third District, the influence
of this agency is more distinctly visible. *
From the quarries on the Seneca outlet, to the west of Waterloo, this rock does not again
appear for several miles, having evidently been excavated in a direction north of Seneca lake,
for about the same width as the lake. At Jones' quarry, where it first appears, in the town
of Phelps, its eastern edge forms nearly a perpendicular escarpment, showing either a sinking
down of the rock on the east, or its entire removal. The latter seems more probable, since
there appears no evidence of causes to produce the former, and there are many reasons and
facts for inferring that the valley of Seneca lake once extended much farther north than at
present. - - - -
In Ontario county, at the place just mentioned, the rock is nearly of the same color and
character as in Seneca county. Farther west it becomes of a lighter grey color, and often
exhibits a tendency to crystalline structure. At the numerous points along this terrace west-
ward where this rock appears, it presents a rounded outline of a light grey or almost ashen
color, with projecting nodules or layers of hornstone, which, from weathering, have assumed
a yellowish color, and are checkered by seams in all directions. Near Oakes' Corners, the
course of the railroad has cut through its northeastern extremity; and along the south side of
the railroad, for some distance, its northern outcrop is visible.
At Vienna, the whole rock is well exposed in the bed of the stream, extending from the
lower to the higher village, and appearing still farther beyond. -
The strata resting upon the Onondaga limestone are principally composed of hornstone;
the calcareous matter has been dissolved from the same, and it presents the most rugged and
irregular appearance conceivable. Where the stream passes over these beds, the calcareous
portions are worn much deeper, while the hornstone stands up in projecting knobs. The lower
part of the mass is developed in about twelve distinct strata or beds, of about one foot each,
some of them varying from twelve to fourteen inches. The central portion of the mass at this
place has a shaly structure, and is free from hornstone; it contains innumerable small fossils,
which are scarcely distinguishable by the naked eye. This portion of the rock is blue, but
weathers to an ashen color. -
The shaly division is again succeeded by compact limestone with hornstone, and terminates
upward in shaly calcareous, thinly laminated strata. Few fossils are found where the horn-
stone is abundant, but in other parts of the rock they are common.
Two miles west of Vienna, some strata of this rock, containing very little hornstone, are
exposed over considerable surface. The rock is compact, of a light greyish blue color; it is
readily quarried, and furnishes good building stone. The character exhibited in the bed and
banks of Flint creek at Vienna, is the prevailing one along the outcrop of this rock westward.
In the bed and banks of Mud creek, above the village of Freedon, it presents nearly the
same character, except that there is far less hornstone. The central portion is shaly, con-
CORNIFEROUS LIMESTONE, 165
taining the same fossils as at Vienna, and in addition I obtained an Ichthyodorulite about six
inches in length. Some part of the rock above this is very light colored, resembling the upper
part of the Onondaga salt group. This portion, however, is marked by the presence of one
of the most characteristic fossils of the rock, viz. Odontocephalus selenurus. The higher
strata are thin-bedded, but with little intermixture of shaly matter.
The lower part of the rock above Freedon is a fine-grained, compact blue limestone, with
a moderate proportion of hornstone. It contains some thin beds of coarser, greyish, sub-
crystalline limestone; and it is these which in some places become augmented in thickness,
and furnish the fine quarries in this rock. At this place they distinctly alternate with the blue
strata. This character is the same as that presented in the lower part of the rock in Seneca
county, but it offers no sufficient reason for a subdivision. &
Where best developed, the rock presents the threefold division visible on Flint creek and
Mud creek. The same may also be seen in a few other places, but the distinctive characters
are either not persistent, or they are not visible through the whole district. The very fine
grain and light grey color seen in part of the mass on Mud creek, is also visible at one or two
other places, but it is far from being a general or important character.
At Farwell's Mills, and at West-Mendon, the same general character of the rock is exhibited.
The proportion of hornstone varies at almost every locality, but usually some of the strata
consist in large proportion of that mineral. At Avon the higher strata of the rock have be-
come a compact thick-bedded stone, and being entirely free from hornstone, are quarried in
considerable quantities. The lower part of the mass has been exposed near the same place,
and contains abundance of hornstone. -- -
It is quite unnecessary to follow all these local variations in the character of the rock. From
what is already said, it will be plainly seen that the nature and proportion of the component
parts vary at different localities. In some places the hornstone predominates through more
than half the mass, while in others it is in very subordinate proportions.
On the west side of the Genesee, its cherty characters are better developed than elsewhere.
Between Caledonia and Le Roy, there are many acres, and I believe hundreds of acres, which
are literally paved with hornstone in small angular fragments, or larger masses united by car-
bonate of lime. In consequence of this stony surface, this part of the town was for a long
time considered almost useless for agricultural purposes, though originally it produced a good
growth of timber, and more recently it has been discovered to be very productive, affording
some of the finest crops. From the nature of the rock, the soil is necessarily highly calca-
reous; and from the abundance of stones, the surface is kept at a more equable temperature
than in some other soils.
The manner of destruction produced by weathering is very obvious in this rock: the cal-
careous matter dissolves away; the hornstone, as it projects, shows little interstices or cracks,
which are soon filled with water, which, on freezing, enlarges the space, and thus after a time
the whole mass is broken down. This process is readily understood by an examination of the
rock at any of its outcropping points. The roads over this portion of the rock are superior to
166 GEOLOGY OF THE FOURTH DISTRICT.
the best macadamized roads; the loose arrangement of the fragments allowing the percolation
of water, which is drained off by fissures below. The siliceous matter soon becomes pul-
verized, and offers no inconvenience from the size of particles. If man would take a hint from
nature's operations, the more cherty parts of this rock would be used for improving the roads
along the whole line of its outcrop. Still the only place where this mode of improvement has
been adopted, is on the road from Buffalo to Williamsville.
The general characters of this rock are seen along the main road from Caledonia to Le Roy,
and the country intervening this line and the northern margin of the terrace. Its rough and
jagged surface everywhere marks its occurrence, and along this distance its development is
greatly superior to that of the Onondaga limestone. -
About two miles southeast of the village of Caledonia, on the land of Mr. Christie, the
compact grey portion of this limestone is well devoloped, forming thicker strata thanelsewhere
in the district. It has been extensively quarried for the Genesee Valley canal. In appearance
it much resembles the Onondaga stone; but the presence of large quantities of hornstone,
and the occurrence of some fossils peculiar to the corniferous rock, are conclusive evidences.
In the bed of the stream below Le Roy village, the Corniferous rock prevails to the almost
entire exclusion of the next mass below. The section along this creek gives between thirty
and forty feet by actual measurement, which is composed almost entirely of limestone. This
section in detail is as follows, beginning with the highest stratum of the rock, which is suc-
ceeded above by the Marcellus slates.
FEET. INCHES.
Two strata of grey limestone with numerous fissures, slaty, and compact at different
points . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 1 8.
Compact grey limestone—two strata . . . . . . . . . . . . . .* - - - - - - - - - - - - - - tº e º e º e e s tº 2 4
Hornstone with little limestone . . . . . . . . . . . . . . . . . . . . . . . • * - - - - - - - - - - - - - - - - - 0 8
Limestone . . . . . . . . . . . . . . . . . . . . . . . . © e º O e º ſº e º e º 'º e º ºs e º e º e º e G © tº e º e º e e º º 1 5
Hornstone . . . . . . . . . . . . . . . . e tº e º a º e G . . . . . . . . . . . . ... . . . . . . . . . . . . . . . . 0 4
Limestone . . . . . . . . . . . . . . . . . . . . e e º e º ºs e º e º 'º e º e . . . . . . . . . . . . . . . . . . . . . . . . 0 10
Hornstone ... . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ... e º e º e e º e º 'º e G . . . . . . . . . . 0 14
Grey limestone . . . . . . . . * @ e º e º e º 'º e e º e & e º 'º e º e e º e e . . . . . . . . . . . . . . . . . . . . . . 1 6
Hornstone . . . . . . . . . . . • e º e º a º e 9 • e o 'º e º e º e º e º e º e º e º e º e e º 'º • * * * * * * ... . . . . 0 3
Limestone .......................................................... 0 9
Hornstone . . . . . . . . tº º e º e º te e e • * * * * * • - - - - - - - © e º e º e Q e e º 'º e º e º e º e º e º e º e º 0 3
Grey compact limestone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2 0.
Thinly laminated limestone with fossils. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 2 0
Compact limestone with fossils .......................................... 2 0
Limestone with nodules of hornstone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 1 6
Limestone . . . . . . . . . . . . . . . ........................................... 0 6
Hornstone . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 0 4
Limestone in two courses . . . . . . . . . . . . . . . . . . . Q @ e º e º 'º e º 'º º e º º e º e º e º º tº & © e 1 10
Limestone with nodules of hornstone, in two strata separated by hornstone ....... 3 2
Limestone in courses of one foot each, separated by layers of hornstone ... . . . . . . 6 0
CORNIFEROUS LIMESTONE. - I67
- * FEET. INCHES.
Limestone in two courses, with an irregular layer of hornstone between . . . . . . . . . 2 2
Thin-bedded limestone with much hornstone innodules and flattened masses, all con- -
taining abundance of coralline fossils. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ... 3 0
Limestone with a large proportion of hornstone intermixed; contains some coralline
fossils ... . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ... 10 0
Limestone in two courses of ten inches each.............................. c. 1 8
From this point there is a fall of twenty or thirty feet in the stream, where the rock
is indistinctly seen. From the point where it reappears, there are thin strata of
hornstone with a small admixture of calcareous matter, the whole exceedingly
rough and ragged . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 24 0
The last division contains in its upper part numerous coralline fossils usually replaced by
silex, and in many instances they are even more durable than the mass of hornstone around
them. The lower part of this mass is separated from the Salt group by six feet of light grey
limestone, destitute of fossils, which, from its position, represents the Onondaga limestone.
There is no other point known in the district, where there is so great a development of the
hornstone of this rock, it usually being a very subordinate part of the whole. From the vici-
nity of Le Roy, there appears to be a gradual diminution of the siliceous matter in a westerly
direction, some points being nearly free from it. Within ten miles of the Niagara it again
increases, constantly augmenting as far as Black Rock. In this intermediate space it occurs
mostly as nodules embraced in the calcareous rock, and sometimes increasing so as to form a
separation between the layers. The rock is usually of grey or greyish blue color; but when
within ten miles of the Niagara, it again assumes the very dark, almost black color of the mass
in Seneca county. i
At Black Rock, where so well developed, the mass consists of calcareous matter in irregular
wedge-form layers, separated by thin laminae of shale. In some instances the siliceous por-
tions are equal to the calcareous, and both are blended in the most heterogeneous manner.
It is separated from the terminating rock of the Salt group, by a layer of grey limestone about
fourteen inches thick. 3. - - -
It will be observed, that in all cases where this rock is highly developed, the Onondaga
limestone, the next rock below, is but meagrely so. For all practical purposes, in the Fourth
District, the two masses may be considered as one. They are intimately connected, forming
together the Limestone Terrace, and there are few good localities where both are not to be
seen. In lithological character, there is scarcely more difference between the Onondaga and
the Corniferous, than in different parts and different localities of the latter rock.
The fossils of the two rocks in many instances blend together, or more properly the Favo-
sites and other corals of the Onondaga occur in the central part of this rock. The upper part,
however, is always distinguished by its organic contents, as will be seen under that head.
Localities. – The occurrence of this rock almost continuously through the district, offers
numerous localities for its examination. A few of these may be indicated, as affording better
168 GEOLOGY OF THE FOURTH DISTRICT,
exhibitions of the strata than others. The numerous quarries mentioned in Seneca county,
are all interesting localities. The bed of Flint creek at Vienna, the outlet of Canandaigua
lake, and the bed of Mud creek, all offer interesting points for examination. At the village
of West-Mendon, the strata are well exhibited, though few fossils occur. To the south and
west of the village of Caledonia, and the whole distance between this point and Le Roy, there
is a fine exposure of the rock. The bed of Allen's creek at Le Roy, as far as the falls, affords
perhaps the best exhibition of the strata in the district. At Clarence Hollow, this rock con-
tains a few fossils not elsewhere seen. In the vicinity of Williamsville, and at several points
between this place and Buffalo, to the south of the turnpike, the upper part of this rock is well
developed. It is peculiarly interesting from containing numerous fossils of the genera Stro-
phomena, Delthyris, and Pleurorhyncus. At Black Rock, the lower part of the mass is very
fully developed, and presents many interesting fossils. -
The places enumerated will give a very perfect idea of the character of this rock; indeed,
two or three of these localities are sufficient to present its most characteristic features.
Thickness. – The point of greatest thickness actually measured is on Allen's creek, where
it is seventy-one and a half feet. At the eastern extremity of the district, the thickness can-
not be more than half this, and at some points I have estimated it at thirty feet. At Black
Rock there is about twenty-five feet laid open to view; but the higher part of the rock is not
visible, and from the deep alluvion covering it farther east, it cannot be correctly estimated.
The increased thickness in many instances seems due to the augmentation of the hornstone,
which is exceedingly variable, often being collectively less than six feet, and again amounting
to four or five times as much.
Mineral contents of the Corniferous limestone. — The mass presents few simple minerals,
besides those which form an essential part of its composition. The hornstone sometimes
passes into chalcedony, and crystallized quartz is rarely found. In the cavities in this rock
at Black Rock, dogtooth spar sometimes occurs. Fluid bitumen, or petroleum, occurs in the
same situation, usually filling the cells of the Favosites, from which, when broken, it often
exudes in considerable quantity.
Springs.
This is one of the most interesting rocks in regard to the production of springs. As before
described, the rock is crossed by vertical joints in two directions. The planes of these joints
are usually separated several inches, and often several feet toward the northern margin of the
rock; and by enlargement within, they sometimes form the entrance to a cavernous expansion.
The soil above being usually thin, the water readily finds its way into these fissures, and passes
off beneath. From this circumstance, it is often difficult, or nearly impossible, to obtain water
by digging wells, unless the rock is blasted to great depth.
The water passes downward till it comes to an impervious stratum, where it is held up, and
rising in the fissures till it can find some outlet, gushes out at the northern edge of the escarp-
CORNIFEROUS LIMESTONE. I69
ment, in the form of numerous copious springs, which are among the most prominent, as they
are often the most interesting and refreshing feature to the toil-worn geologist, as well as to
the inhabitants of the place. The upper part of this outcropping edge often presents the most
dry, barren, and uninviting appearance; while a few feet below, the surface is fresh and
green, the soil moist, and little springs gushing out at every step. -
The process by which these springs are produced, will be understood by the following
diagram :
66.
The water passes down through the fissures a, a, to the impervious stratum c, where it ac-
cumulates till of sufficient height to flow over its northern edge at e, forming springs which
are constantly supplied from the inexhaustible fountain in the fissures and cavities of the
limestone. The water often accumulates in these fissures to a considerable height above the
spring, particularly where the face of the cliff A is deeply covered with drift.
On the land of Mr. Stevens in the town of Clarence, Erie county, there is a broad fissure
by which one can descend to a cavernous opening below. This in the spring, or during rainy
seasons, is filled to within a few feet of the surface with water, which during the dry season
of summer gradually subsides, as the discharge by the springs is greater than the supply from
the surface. During the winter and spring, from the rains and dissolving snows, these fissures
become quite filled, and frequently the water rises above the surface, forming little ponds in
depressions half a mile south of the outcrop, in the position of 4, 4. At these seasons a greater
quantity flows out by the springs and other openings on the north than usual, and the equili-
brium is soon restored.
Where the soil is thin above the limestone, the course of these joints is indicated during the
dry season by the freshness of the grass and herbage growing along their direction. The
evaporation of the water below moistens the soil covering the joints, and consequently it
retains the same freshness as where moistened from above, while the surrounding portions
become dry and parched. Where the rock is thin and more deeply covered with soil, these
features are not discernable. Y
In several instances streams flowing over this rock disappear in the fissures, and afterwards
reappear at some more northerly point. Allen's Creek, at Le Roy, disappears in this manner
a little north of the village, so that in summer and autumn the bed is entirely dry below.
After thus disappearing, it evidently takes some other course, for it does not appear in the
same channel below the falls for some distance. It is a favorite belief with many that this
[GEOL. 4th DIST...] 22
170 GEOLOGY OF THE FOURTH DISTRICT,
stream rises again in the Caledonia spring, seven miles distant; but the only facts advanced
are the disappearance of the one, and the occurrence of the other with no apparent origin.
The Caledonia spring, from the great quantity of water it affords, is evidently the common
outlet for a large area in its vicinity; but whether it is supplied from so great a distance as
Le Roy, may be questionable. To the west and southwest of Caledonia the surface in wet
seasons presents numerous small lakes or ponds, which drain off into the fissures below; and
it is evident, from the nature of the rock, that there is a large reservoir constantly maintained.
The springs at Canoga, in Seneca county, owe their origin to the same cause, as also those
at Springport, on the opposite side of the lake.
Agricultural characters.
The character of the soil covering this rock varies, to a considerable degree, according to
its development. Where the rock is thin, as in the eastern part of the district, it scarcely
produces any effect upon the surface; but where thicker, it has essentially modified the charac-
ter of the soil. In Seneca county the soil covering the northern part of this rock is clayey,
but becomes more loamy toward the southern part; in the western and central part of the
county it is frequently covered with a loamy soil, but the characters appear entirely due to
the accumulation of northern drift.
Where the rock becomes thicker and the quantity of hornstone greater, it has produced a
coarse siliceous or silico-calcareous soil, from the destruction of the rock in the manner before
described. The surface in such cases is often forbidding, from the great quantity of frag-
ments of the “chawed rock,” as it is termed; but where the larger of these are removed, the
soil proves of the best quality. The constant destruction of the larger fragments by the
action of frost and water liberates fresh calcareous matter, which must constantly act as a
fertilizer.
Organic Remains of the Corniferous Limestone.
The central and lower portions of this rock usually exhibit few forms which are peculiar to
it, though they serve, from their association, to aid in the identification. In the higher por-
tions, which are nearly or entirely free from hornstone, the fossils are peculiar, and serve at
once to identify the rock, being known in no other. Among these fossils are two trilobites, the
Odontocephalus selenurus of Green, and a Calymene. So abundant is the former of these
at Schoharie and other places, that it alone is the fossil entirely relied on, and the rock is
known as the “Selenurus Rock.” The other trilobite is scarcely less characteristic. In
many places in the Third District, and in Seneca county in the Fourth District, the Stropho-
mena lineata of Conrad is the typical fossil, but it rarely occurs at any point west of the last
named locality. - - . .
There are several species of the genus Cyrtoceras which are apparently confined to this
rock, and in the eastern part of the State are common, while in the Fourth District they are
but occasionally seen, other forms taking their place.
CORNIFEROUS LIMESTONE, t - I71
The following illustrations present some of the most common forms of this rock in western
New-York, though there are many others which perhaps are equally abundant.
§ º - § §
fººt §
§: -
*: º:
{{#S -
§§§ §§
W
WS
1. Atrpya Scitula. 4. Strophomena crenistria. 6. Pleurorhyncus trigonalis.
2. Paracyclas elliptica. 5. Delthyris duodenaria. 6 a. Pleurorhyncus trigonalis.
3. Strophomena acutiradiata. - Y
1. Atrypa scitula, n. S.–Obovate, compressed towards the base; lower valve very convex,
with a produced incurved beak; upper valve convex in the middle, with a small, rather pro-
minent beak. The shell is very glabrous, with faintly perceptible concentric lines; it may
be distinguished from any other in the rock, by the extension of the beak of the lower valve.
Locality—Williamsville, Erie county.
2. Paracyclas elliptica, n. S. – Shell broad oval; beaks scarcely prominent ; surface
marked by concentric lines; valves equally convex; very much elevated on the umbones.
Shell the size of the figure, and larger; it is readily distinguished by the figure alone.
I am indebted to Dr. Everitt, of Batavia, for specimens of this fossil.
Generic name from its similarity to the Cyclas.
Locality—Le Roy, Genesee county.
3. Strophomena acutiradiata, n. S. – Lower valve convex, slightly impressed in front and
on each side; hinge line extended beyond the width of the shell, and obtusely angulated at
the extremities; surface covered with sharp striae, which bifurcate toward the margin.
Locality—Five miles east of Buffalo. Very abundant in the higher strata of the rock.
4. Strophomena crenistria, n. s. – Semi-oval; lower valve slightly convex; upper one
nearly flat; surface covered with fine diverging striae, the spaces between which are crossed
by concentric lines; upon the striae, these lines produce elevated points or crenulations; hinge
22*
I72 GEOLOGY OF THE FOURTH DISTRICT.
line slightly arched, extending beyond the width of the shell, and obtusely angulated. The
surface is marked by a few concentric lines of growth.
See also a figure of the same shell in the Hamilton Group.
Locality—Vienna, Ontario county.
5. Delthyris duodenaria, n. S. – General figure semicircular; valves nearly equally con-
vex: mesial fold much elevated towards the front; ribs 12, gradually decreasing in size from
the centre, rounded, and crossed by concentric undulating lines.
The specimen is imperfect, and though the fossil is abundant, I have never been able to
obtain a perfect one. It is readily known by the number of its ribs and the undulating lines.
Resembles D. raricosta of Conrad, the D. undulatus of Vanuxem (Report, p. 132), but differs
from that in form and in the number of ribs. Concentric lines often obsolete.
Locality—Five miles east of Buffalo, and at other points on the Macadam road.
6. Pleurorhyncus trigonalis, n. S. — Sub-triangular; beaks little elevated; surface marked
by about 20 ribs, some of which are divided; anterior surface broadly cordate; posteriorly
slightly elevated and conoidal. -
2 a. A view of the base, showing a portion of the shell remaining, which extends anteriorly
beyond the cast, and is striated. This appears like a kind of sheath, which has apparently
no opening upon the base.
This shell is certainly unlike the P. cuneus of the Schoharie grit.
Locality—Williamsville, Erie county.
º
º ſ
%iº ^
§§ ſ - \\\\\\\\\ § \ § j º |||}|| º: y
%| º - º
%iº Wºº
%/|| Wº Ǻ
% ſº | |ft||| ###### # 4. W * §§ a- -
1 Pterinea cardiiformis. 3. Orthonychia. 5. Calymene crassimarginata.
2. Tentaculites scalaris. 4. Euomphalus? rotundus. 6. Acroculia erecta.
CORNIFEROUS LIMESTONE, 173
1. Pterinea 2 cardiiformis, n. s. – General figure cordiform ; valves equal ; posterior
margin alate; cast of wing gibbous; surface marked by fine radiating striae, and crossed by
prominent lines of growth; beaks large and prominent. Wing imperfect in the specimen
figured. -
The shell is perfectly preserved upon the specimen figured, which is from the cabinet of
Mrs. Ransem of Clarence Hollow. Several perfect casts were found in the same vicinity. It
closely resembles a species of this genus in the Oriskany sandstone. It is with some hesita-
tion that I refer this fossil to the genus Pterinea, being inclined to consider it distinct.
Localities—Clarence Hollow, and one mile west of this place.
2. Tentaculites scalaris, SCHLoTH. (Silurian Researches, p. 643, pl. 19, f. 16.) — Sub-
ulate; composed of a series of truncated cones, with their bases towards the apex of the shell.
Each higher joint appears to proceed from within the one below, “forming a set of steps
rather than rings, like the sliding joints of an opera glass.”
In England this fossil is abundant in the Caradoc sandstone, as it is in New-York in the
Hudson river group; and Mr. Murchison remarks, that “it is not possible to distinguish this
body from the Tentaculites of the Ludlow formation.” The one figured holds a place more
nearly equivalent to the latter formation. -
Locality—Le Roy, Genesee county.
3. Orthonychia."—Tapering, slightly curved above; obtusely angular, having the form of
a claw or talon, as the generic name indicates. x
There are several forms similar to this in the limestones of the Helderberg division.
Locality—Near Williamsville, Erie county.
4. Euomphalus? rotundus, n. S. – General form spheroidal; last whorl very much ex-
panded; rapidly tapering to the summit, which is moderately elevated; umbilicus large.
The figure is from a cast. Shell striated. - :
Locality—Clarence, Erie county. - * , x *
5. Calymene crassimarginata, n. S. — The abdomen and caudal portion of this fossil is of
frequent occurrence in this rock. There are about sixteen articulations visible in the middle
lobe, and two or three more on the lateral ones. It is distinguished by its great convexity,
the prominence of the middle lobe, and the thick margin. The middle lobe is rather flat, and
the articulations extend nearly straight across, bending more suddenly down at the sides. The
articulations toward the extremity are often scarcely visible in the cast.
This fossil is one of those forms typical of this rock throughout Ohio, Indiana and Rentucky.
Localities—Near Williamsville, Clarence, Caledonia and Avon. -
* A new genus, which I have adopted on the suggestion of my friend Mr. S. S. HALDEMAN, and which will include
several forms analogous to this. See forthcoming Palaeontology for description. -
174 º GEOLOGY OF THE FOURTH DISTRICT.
6. Acroculia erecta, n. s. – Erect; incurved at the beak, forming nearly two whorls; ra-
pidly expanding below. The surface is sometimes crossed by undulating lines. This is by
no means a rare fossil, though sometimes less incurved at the apex. -
The form of the fossilis perfectly represented, though its more minute characters could not
be, in consequence of the badness of the wood. - -
Localities—Five miles east of Buffalo, Williamsville, Le Roy and other places.
69.
º *
l
t
º
Sºº-
|
Śº
ſº
|
YūWTT". - ſº *Tº Tºr-amº-rºmyº-"
rºº ſº lºº
W surrº, \!. º § _2:\ - tºllſ
JMrs. Brooksáez.
Ichthyodorulite.
The illustration above is the most perfect specimen of this kind of fossil seen in the district.
The specimen is slightly arched, and carinated upon the back; the surface is marked by
parallel grooves and ridges, which extend nearly to the point; the latter is smooth, and finely
finished. The specimen is 5% inches in length.
Locality—Freedon, Ontario county.
There is a much larger specimen of a different species, in the cabinet of David Thomas of
Aurora, which was obtained at the quarries near Waterloo. Mr. Skaats of Geneva informs
me that he has seen a specimen from the Waterloo quarries, more than eight inches in length,
and curved nearly into a semicircle. The surface was smooth, except an angular ridge along
the centre. - -
CORNIFEROUS LIMESTONE. 175
The following woodcut is from the Report of Mr. Vanuxem, and exhibits the prevailing
forms in this rock in the Third District:
* -
g -
º
ſº wº
|\º
§§ w
º
N § º
% §
% § Nº
§ ſ §
*: º d º
%|\\
§§ºliº:
% § #º
º §.”
- º §§
ºft#. §
§ Hºlº
§§ sº
ſ
º
%; $º W § §§§
jº
º
§º - Nº §
º §
º
1. Odontocephalus selenurus. 3. Strophomena undulata.
2. Cyrtoceras undulatum. 4. Orthis lenticularis. 8. Strophomena lineata.
5. Atrypa prisca.
1. Odontocephalus selenurus. – The post abdomen and caudal extremity are of frequent
occurrence in the Fourth District. -
2. Cyrtoceras undulatum. — Specimens of this genus have been seen at Waterloo, Cale-
donia and Le Roy. -
3. Strophomena undulata. — This is a common fossil in many places, usually tinged of a
reddish or bronze hue.
3. Orthis lentiformis, has not been seen in the district.
5. Atrypa prisca, is one of the most common and abundant fossils.
6 & 7. Ichthyodorulite, and section of the same. This has not been seen in the district.
8. Strophomena lineata. — This is an abundant fossil in Seneca county, but is very rare
farther west.
Nos. 1, 3 and 8, may be considered as characteristic fossils in the Fourth District.
With the termination of the Corniferous limestone end all the important limestones of the
New-York System. The calcareous deposits which occur in a higher position are, for the most
part, thin and rarely persistent over a great extent. The constancy and wide extent of the
beds just described renders them one of the best horizons of reference in the whole system.
The subsequent deposits are of a nature quite different, and the organic contents are, for the
176 GEOLOGY OF THE FOURTH DISTRICT,
most part, unlike those of the limestones. Over the whole area known to be occupied by the
Corniferous limestone, there is an abrupt change from that rock to a black fissile argillaceous
slate; while fossils, which have been abundant in the limestone, either cease entirely or are
succeeded by others of a totally different character.
The Marcellus shale is the commencement of what may be considered as one great period
of the New-York system, the materials of which are very unlike in different parts, or isolated
portions; but viewed as a whole, present a general similarity in the products and their causes.
The variation in lithological character is attended by a greater or less change in the character
of the fossils; and though every successive division is strongly marked by its peculiar organic
types, still some species of the lower divisions may always be found. The line of demarka-
tion between these divisions is sometimes, and in some places, well defined, while at others
there seems a gradual merging not only of the lithological products, but also of the fossils.
The divisions heretofore enumerated in the Fourth District are sufficiently well marked
throughout its extent, while at the east they are gradually less distinct, until at last in many
places there is no distinguishable line of separation.
This arises both from the greater similarity of lithological products throughout, which the
whole presents at the east, and also from the gradual ascent of some of the fossils which at
the west are confined to lower divisions. This will be made more apparent under the descrip-
tion of the several subdivisions.
The whole series, from this point as far as the base of the Old Red Sandstone, seems to have
been coéval and coéxtensive. All the members gradually diminish in thickness in a west and
southwest direction, and the fossils of all seem to keep pace with this diminution, until at last
the mass is nearly or quite non-fossiliferous. At their eastern commencement the lithological
character is similar throughout the greater part of the mass, but as we progress westward we
find a gradual separation, the more shaly portions with some calcareous matter taking the
lower position, while the sandy and the alternations of shaly and sandy deposits hold a higher
place. This character is maintained nearly the whole distance to the Mississippi river.
MARCELLUS SHALE, 177
\.
23. MARCELLUS SHALE.”
Lower part of the Pyritiferous rock (Third Graywacke) of Eaton. Marcellus shale and
Black Shale of the Annual Reports. -
(Lower PART OF No. 8, PENNSYLVANIA SURVEY. BLACK SLATE of THE OHIO REPorts.)
[See Sections Plate 7 and Plate 13, No. 3 and 4; also woodcut, page 27.]
This rock admits of two divisions. The lower is very black, slaty and bituminous, and
contains iron pyrites in great profusion; some portions are calcareous, and it is always mark-
ed by one or more courses of concretions or septaria, which are often very large. This
division terminates upwards by a thin band of limestone, above which the shale is more fissile,
and gradually passes from black to an olive or dark slate color.
In general characters the lower part resembles the Utica slate, and is not distinguisha-
ble from the Genesee slate in its general aspect; it is, therefore, more properly a slate than
a shale, if the distinction is to be continued. For practical purposes, there is little advantage
in separating the upper division of this shale from the Hamilton group. The line of separa-
tion is nowhere well marked, the change in lithological character being gradual, while some
of the fossils continue from one to the other.
The finely levigated mud composing this rock indicates a period of great tranquillity in the
waters, moved probably only by currents sufficient to transport the materials over the wide
extent we find them. The nature and condition of the fossils also indicate a quiescent period;
for their forms are among the most delicate, and their parts are usually preserved in the
greatest perfection. In some instances, however, from their great numbers, they are packed
closely together, and fracture on the separation of the laminae.
This rock occupies the depression which extends along the southern border of the Cornife-
rous limestone, and from two to three or four miles south of its outcrop. From its soft and
destructible nature, it is only exposed in ravines and water courses, and from these situations
we obtain a knowledge of its characters. The lower part, when long exposed, weathers to
a brownish or iron rust color, partially from the presence and decomposition of iron pyrites,
and partially from bituminous matter. In some situations it retains its purely black color,
and scarcely separates into slaty laminae after long exposure.
In many places, this rock contains so much bitumen as to give out flame when thrown into
a fire of hot coals. From this character, and its black color, it has been considered an in-
* In Ohio, Kentucky and Indiana, a rock possessing the same characters, and apparently holding the same place as this one,
is known as the “Black Slate;” and this term seems more appropriate than Shale, since the rock is everywhere slaty in
structure. In lithological aspect it is undistinguishable from the Genesee slate of New-York; but since the term Shale has
been adopted, it is followed in this report.
[GEoL. 4th DIST.] 23
178 GEOLOGY OF THE FOURTH DISTRICT.
dication of coal; and throughout the district, and even the whole length of the State, it has
been bored or excavated in search for this mineral. This example affords an exemplification
of the reasoning and practice in the absence of geological knowledge, and shows most clearly
the benefits which may be derived from understanding the order among our rocks, and the
true place of the coal-bearing strata. - -
This rock first appears in the district in Seneca county, where it succeeds the Corniferous
limestone. There are one or two natural exposures of the same south of Waterloo village,
and it approaches within a few feet of the surface entirely across the county. The portion
most exposed is black and very fissile, separating into thin laminae, from the presence of great
numbers of a smooth Avicula, which is everywhere an abundant fossil of this rock. It is
exceedingly thin and fragile, and usually appears in fragments upon the surface of the laminae.
Its form is obscure, though when perfect there is no doubt of its character.
In the excavation of wells a short distance south of the point where the limestone disappears,
this shale is usually thrown out; and it can always be distinguished by the shell just men-
tioned, and flattened fragments of an Orthoceras, as well as by its peculiar black color.
The same rock appears about two miles south of Vienna, in the banks of Flint creek. The
portion exposed is very fissile from weathering, and its color externally is somewhat greyish.
The same thin stratum of limestone which holds a place in the shale in other places, appears
at this locality. It contains a large number of Orthocerae and a species of Euomphalus, but
the interior is usually lined with crystalline matter, and the shell is very fragile. At this place
I found a fragment of the Dipleura Dekayi, which is the lowest position in which I have seen
this fossil. The shale also appears about two miles southeast of Vienna, and near the point
where the limestone disappears beneath the surface.
The bed and banks of Flint creek in Bloomfield exhibit this rock in a good degree of per-
fection, and well marked by its peculiar fossils. The outlet of Conesus lake, a little west of
the village of Avon, is one of the best exposures of the rock in the district. The lower part
is black and fissile; about twenty feet higher, the mass is more compact, very black, and
highly bituminous. It contains large accretions of siliceous limestone, which are sometimes.
quite pure, at others intermixed with shale. The stratum of limestone is compact, about a
foot in thickness, and filled with fragments of fossils. The rock just below and above this
limestone is very fissile, readily separating into broad slaty laminae, the surfaces covered with
organic remains. - *
On the west side of the Genesee river, it appears about two miles south of Caledonia village,
where it has been bored in several places in search of coal. At this place, and a short dis-
tance farther north, it presents its usual characters both of compact and fissile structure.
At Le Roy village, this rock is well exposed to view in the bed of Allen's creek. The
lower part of the shale is mostly compact, with little tendency to lamination, while the higher
portions are very fissile. It contains a great abundance of concretions or Septaria, which are
plentifully distributed through the mass at about the level of the creek, and below the fossili-
ferous portion of the rock. These concretions are of a siliceous limestone, apparently resulting
from a small quantity of the material spread over the surface, which being too little to con-
MARCELLUS SHALE. - 179
stitute a continuous stratum, assumed this form. The continuous stratum of limestone before
noticed appears at this place, having the same character as elsewhere. The shale above it is
very fissile, separating into thin laminae, and abounding in fossils.
The lower part of the mass, on weathering, becomes iron-stained; but that portion above
the limestone weathers to an ashen hue. : -
A little west of the village, the shale approaches the surface so nearly that it blackens the
soil along the road. -
West of Le Roy, there are few good points where this rock can be seen. The great depth
of alluvion about the point of its junction with the Corniferous limestone has generally obscured
the lower portion. At Alden and a few other points in Erie county, the upper part of the
slate, abounding in Tentaculites, can be seen. The deep excavation along the valleys of
Cayuga and Seneca creeks near Buffalo, and the depth of the drift and alluvion, effectually
conceal this rock, though the Hamilton group above is well exposed. -
Localities.—The two principal localities in the district, and those to which an observer
should direct his attention, are the ravine of Conesus outlet, a little west of the village of Avon;
and the bed and banks of Allen's creek, near Le Roy. At the former place, the absolute
contact of the Marcellus shale with the limestone below is seen beneath a sawmill, where the
rock is exposed. Its extent upwards is well exhibited, and its peculiar fossils can all be ob-
tained. At Le Roy the same features are exhibited, and its connexion with the limestone is
distinctly seen. × -
There are no other localities in the district, where the connexion with the lower rocks, and
the characters of this, are so well exhibited. -
Thickness. – The greatest thickness of this rock, where it can be measured accurately,
does not amount to more than fifty feet; but as before stated, it gradually merges into the
olive shales above. In the Third District, this shale is much thicker.
Minerals. – This rock contains no minerals of importance. Sulphuret of iron is every-
where found. Sulphate of baryta often occurs in the septaria, and crystallized carbonate of
lime in the same situation, and lining the cavities of fossil bodies. r
Springs. – From the presence of iron pyrites, the water flowing over, or rising from fis-
sures in this rock, is often charged with sulphuretted hydrogen, though there are no copious
springs. *
Agricultural characters. — The shale alone, on decomposing, produces a clayey soil; but
its width being small, and the accumulation of drift at this point being excessive, it rarely gives
character to the surface soil for any considerable extent.
23%
%
180 GEOLOGY OF THE FOURTH DISTRICT.
Organic Remains of the Marcellus Shale.
Nearly all the fossils are of small size and very delicate structure, indicating, as does the
finely levigated mud in which they are imbedded, a quiet condition of the ocean in which they
lived. These delicate forms are preserved in the greatest perfection, the most fragile shells
being often as perfect as when living. .
This character of small size of the fossils does not apply to the rock everywhere; for in
the Third District it contains some goniatites, larger than in any other rock in the State.
The more common fossils met with, and those which are typical of the rock, are presented
in the following illustration. So far as can be ascertained, these forms are all undescribed,
with the exception of the last, which was named in the Report of the Third District. These
occur at the two localities mentioned as the best points of observation, where they are very
abundant, as well as many others not here figured.
71.
2% º
º lºmºmºrº Š
º º º º º º
1. Orthoceras subulatum. 4. S. pustulosa. 7. A. equilatera. 10. Tentaculites fissurella.
2. Strophomena setigera. 5. Avicula muricata. 8. Orthis nucleus. 11. Atrypa limitaris.
3. S. mucronata. 6. A. laevis. 9. Orbicula minuta.
1. Orthoceras subulatum, n. S. — Shell tapering to an acute point, smooth; septa nume-
rous, slightly arched on each side of an impressed line, which extends the whole length of
the shell. There is usually about one-third of the shell where no marks of septa are visible.
This fossil is usually much flattened, and often replaced by iron pyrites, which from de-
composition prevents the septa from being visible. It is apparently the only species in the
rock. -
Localities—Bloomfield, Le Roy, Avon, Seneca lake.
2. Strophomena setigera, n. S. – Shell semi-oval, marked by numerous fine radiating striae,
and a few concentric lines of growth; beak scarcely elevated; hinge line with six flexuous
spines, which appear like bristles. The extent of the hinge line is proportionally much less
than in S. cornuta of the Clinton group; the striae are also coarser. .
N. B. The spines are too short and rigid in the figure, but there has been no time to have
it reëngraved. .*
Locality — Avon.
MARCELLUS SHALE. *. #8;
3. Strophomena mucronata, n. S. — Shell semi-oval, with coarse striae, which radiate from
an imaginary point beyond the beak; beak of the lower valve elevated ; hinge line extended
into a kind of spine.
This shell is readily distinguished by its coarse striae, which do not radiate from the beak,
and the peculiar extension of the hinge line.
Localities — Avon, Indian reservation, Erie county.
4. Strophomena pustulosa, n. s. —Shell semi-oval, contracted beneath the hinge line; sur-
face covered with wrinkles and pustules, without striae; hinge extremities angulated.
The surface appears as if it may have been covered with spines, but I have not been so
fortunate as to observe them. The shell when present is of a pearly hue, and readily sepa-
rates, leaving a cast of the fossil. It is quite abundant.
Locality — Avon, Livingston county.
5. Avicula muricata, n. S. – Obliquely ovate; surface marked by elevated, radiating and
concentric lines, giving a cancellated appearance; from the junction of these lines rises a short
spine; posterior wing small, produced into a short acute spine; anterior wing obtuse, with
an oblique fold. -
The radiating lines are very faint on the posterior wing, and are not visible on the anterior
wing. The small spines are usually broken off, except on the margin. This beautiful fossil
will be readily identified from the figure.
Locality — Avon.
6. Avicula lavis, n. S. — Obliquely ovate, with the hinge line slightly deflected on the ante-
rior side; beak convex, rather prominent; surface smooth, or marked with fine concentric lines
of growth; posterior wing triangular, abruptly acute, extending nearly in line with the margin
of the shell; anterior wing obtuse, with a slight plication.
This is a beautiful smooth shell, strongly contrasting in its surface with the last, both often
being found together. . \ -
Localities — Avon and Bloomfield.
7 . Avicula equilatera, n. S.— Obliquely semi-elliptical or sub-rhomboidal, nearly flat; hinge
line straight, extending equally on each side of the beak; surface covered by radiating striae,
which are concentrically decussated by numerous elevated lines of growth. * ,
The wings are less distinctly marked than is usual in species of this genus, which with the
equilateral character readily distinguish it. The whole surface is regularly cancellated by the
radiating striae and elevated lines of growth. -
Localities — Avon and Bloomfield.
8. Orthis nucleus, n. S. — Hemispherical; lower valve very convex, with a depression or
sinus from beak to base; upper valve flat, marked with concentric lines of growth, and fine
striae; hinge extremities rounded.
182 GEOLOGY OF THE FOURTH DISTRICT.
This is a very abundant little shell, often forming thin courses, with scarcely the interven-
tion of sufficient shale to make them cohere. It much resembles the Spirifera unguiculus
(PHIL. Paleozoic Fossils, p. 69, fig. 119), and Orthis umbonata (ConFAD, Jour. Acad. Nat.
Sci. Vol. viii, p. 264, pl. 14, fig. 4). The beak is much less prominent, the hinge line less
extended, and the shell smaller than the last named shell.
9. Orbicula minuta, n. s. –Orbicular; surface marked by concentric lines.
This fossil is exceeding abundant, often nearly covering the shaly laminae for several inches
in thickness. They appear like small black specks or points. The larger figure is its maxi-
mum size. It is remarkably persistent in the district, being known at the most extreme loca-
lities. -
Localities–Avon, Le Roy, Bloomfield and numerous other places.
10. Tentaculites fissurella, n. S. — Minute, almost microscopic; annulated above, and
smooth near the base. When sufficiently magnified, a slit is perceived on one side, extending
one-third or more of the whole length. - -
This fossil occurs in myriads, and, although so exceedingly minute, it forms layers several
inches thick, extending many yards, and apparently many miles, it being equally abundant
at distant localities. The layers which it forms are exceedingly fragile, and crumble on the
least exposure to moisture.
Localities–Avon, Le Roy, Waterloo, Alden.
11. Atrypa limitaris. (Orthis limitaris, Geol. Report of Third District, p. 146, fig. 3.)
Compressed, somewhat circular; surface covered with radiating ribs of nearly equal size.
This shell is exceedingly abundant in the upper part of the shale; the stratum, for conside-
rable thickness, is completely charged with them, and they are often associated in great num-
bers with Orbicula minuta. The specimen figured is a fragment of this kind, which presents
the fossil as it usually appears in the rock. It will be readily recognized. :
Localities—Waterloo, Vienna, Avon, Le Roy.
In addition to these fossils, there are two or three univalves which occur everywhere; one
of these is a Goniatite, but from being replaced by iron pyrites which is in a decomposing
state, it is impossible to define it. The large Goniatites figured in the Report of the Third
District, page 146, as occurring in this rock, have not been seen in the Fourth District.
MARCELLUS SHALE. 183
Localities of superposition. g
The following woodcuts illustrate the relative position of this rock in the Fourth District:
Section on the outlet of Conesus lake, one mile west of West-Avon, Livingston county.
Section of the bed and bank of Allen's creek, at Le Roy village.
a. Shale of Hamilton group.
b. Black and olive shale of the Marcellus, gradually passing into that above. *
c. Stratum of limestone with fossils. The shale above and below this limestone is highly fossiliferous.
d. Black bituminous shale with large septaria. Atrypa limitaris occurs in the lowest layers, resting on the limestone e,
e. Corniferous limestone.
a. Shale of Hamilton group.
. Bluish and dark shales of the Marcellus,
c. Stratum of limestone, one foot thick.
. Black slaty and compact shale with septaria, Bed of creek.
e. Corniferous limestone, forming the bed of creek as far as the falls,
§
d
j84 - +. GEOLOGY OF THE FOURTH DISTRICT.
* - 74.
:-------
===:--— ---- =<2*TT-se
2.Éiºã=##$$$.
======#: Éss=s=Sºs
É%% %
%
NS
§ Ş 2
º żº
Š º º } #===# ===ºfflº-E:
º:
Ż
*º-
-º-º-º-º:
º º::::::::::::::::::::::::::
#:::::::::::=#::=::==
E: Erºs:-->.
==E=ºº-ºº:
View of Sugarloaf Hill, at Hopeton, on the Crooked Lake Outlet. From a drawing by Mr. E. N. Horsford.
24. HAMILTON GROUP.
This group at present includes the Pyritiferous rock and Third greywacke of EATON:
Ludlowville, Moscow and Skaneateles shales; Dark slaty fossiliferous shales, Compact
calcareous blue shales, Olive shales, Shales near Apulia and Sherburne; Cazenovia
group, Encrinal limestone, &c. of the Annual Reports.
(PART of No. 8, PENNSYLVANIA SURVEY.)
[See Coast Section of Lake Erie, Plate 5, and Section along Cayuga lake, Plate 7; also O of woodcut, page 27.]
This group consists of several members which may be considered distinct, but which, when
viewed in connexion, present so many features in common, that they are all recognized as the
products of one period, and thus constitute one great group. In the Fourth District, the only
changes recognized in lithological products are from shaly to calcareous, with occasional thin
beds of limestone, and more rarely of Sandy shale.
º
The group, as a whole, presents an immense development of dull olive, or bluish grey cal-
careous shales, which, on weathering, assume a light grey or ashen tint; some portions be-
come brownish on exposure, but these are of small thickness in this district. At a few points
the shale becomes darker, or black, and exhibits a tendency to slaty structure; but as a general
HAMILTON GROUP. 185
character, the cleavage is irregular, and oblique to the planes of stratification. On weathering,
where the edges are exposed, there is manifested a slight tendency to slaty cleavage.
From the wide and even distribution of the materials of this group, it was evidently pro-
duced during a period of great tranquility, when the finely levigated mud was transported over
wide areas by gentle oceanic currents. The great profusion and variety of organic forms
proves also the quiescent condition of the ocean, which, together with the slightly calcareous
nature of the mud, favored the growth and distribution of the Testacea.
The upper part of this group, in the Fourth District, bears a very close analogy in its litho-
logical nature to the shale of the Niagara group; and in abundance of organic remains, it is
even more prolific. The forms of the latter āre, however, of entirely different species, though
corals and shells of similar genera abound, and trilobites of the same and different genera.
Concretions or septaria, in well defined and often fantastic forms, are common in every part
of this group. In many instances the calcareous matter has concreted around some organic
body, or a nodule of iron pyrites seems to have been the centre of attraction. In such in-
stances, we often find numerous fossils imbedded in them, or attached to their outer surface.
The greater number, however, are well defined spheroidal masses, with or without seams of
crystalline matter, and not containing any organic body. Others, and particularly in the lower
part of the shale, are small, spherical or elongated, and with a small perforation through their
centre, in the manner of the common nodules or other concretionary forms in recent clay beds.
Organic forms abound throughout the group, but they vary somewhat in the different parts.
In the lower division, the most abundant are those of Orthis, Atrypa and Strophomena, with
some spiral univalves; while above this portion, great numbers of Avicula, Cypricardia, Nu-
cula, and other similar forms abound, with fewer of the genera Orthis, Delthyris, &c. In the
next division, Delthyris, Strophomena and Atrypa abound, to the almost entire exclusion of
the forms before mentioned. In the same situation with these we find numerous species of
corals: Cyathophylli, Favosites and other forms, are abundant; while fragments of crinoidal
columns are every where scattered through the mass, or spread evenly over the surface, form
thin layers of themselves. Many of the species of this division are discontinued, and their
place supplied by others of the same genera in the higher part of the group. The principal
characteristic forms of each division will be found under the head of Organic remains of the
group. * -
Although this group is so widely spread and evenly distributed, and of uniform character
over the western part of the State, still at its eastern extremity the lithological character is
widely different. The shales are more or less arenaceous, and some parts are well marked
sandstone. The proportion of siliceous and argillaceous earth is nearly reversed from what it
is in the same rocks farther west. The mass varies from sandy shale to shaly sandstone, and
even tolerably pure sandstone. This character gradually changes to the westward, the sand
diminishing and the clay increasing. The features presented by this group at its two extremes,
and along its whole length, offer one of the most instructive exhibitions of the varying character
of mechanical deposits. The facts prove the origin of the materials to have been at the east
or southeast. The force of the current which drifted them into the ocean was sufficient only
[GEOL. 4th DIST.] r 24
186 GEOLOGY OF THE FOURTH DISTRICT.
to carry onward the coarser particles to a certain distance, where they were deposited. The
finely levigated mud was carried beyond this point, being floated by less force than the sand.
Some portion of the clay was deposited with the sand toward the central part of the State, and
but little of the latter extended beyond this point. Finally the current became more gentle,
and the clay was deposited to a certain extent, beyond which the power of the current was
insufficient to carry even this material, and the deposit consequently thinned out in that
direction. -
Nothing could be more analogous than this to the simple operation of a powerful stream
conveying detritus into the ocean. The force of the stream is at once checked as it flows into
the larger body of water, and the coarser materials are thrown down. From this point its
force is gradually diminished as it progresses, and the coarser particles of the remaining matter
are precipitated, until finally it loses its force entirely, and the materials before in suspension
fall to the bottom. Matter like finely levigated clay, however, falls slowly to the bottom of a
deep ocean, and in this way it may be carried on hundreds of miles, although the current be
comparatively weak. -
This is not an isolated example; for the same character is observed in all our mechanical
deposits, which are vastly thicker in one place than another, showing that the ancient ocean
had a limit, and that these materials were brought in like the common detritus of rivers, and
spread over the bottom, gradually diminishing as the force of the current was neutralized by
the greater body of surrounding water.
This change in the nature of the materials is accompanied by an equally marked change in
the fossils imbedded in the different parts of the group. In the eastern part of the State,
Avicula and Cypricardia with Nucula, &c. prevail in immense numbers; while at the extreme
western margin, though in precisely the same position, they are of the rarest occurrence,
while numerous forms of Delthyris and Atrypa abound. In the present state of our know-
ledge of the limits of this ancient sea, it is impossible to say positively what influence proxi-
mity to land or shallow water may have had upon these forms; but it seems, nevertheless,
true that the kind of bottom or bed of the ocean had much to do in modifying the character of
the testacea inhabiting it. Or, perhaps we should say that the different kinds of bottom were
more favorable to the growth of certain species and genera than to others, and that as the kind
of deposit changed, so also did the organic beings inhabiting it." Of this fact we shall find
sufficient proof as we investigate this formation.
* In the present sea we know that its littoral inhabitants, at least, congregate in certain situations and upon certain bot-
toms, and that forms abundant in some situations are rare in others, though different species are abundant. Even the
fishes that approach the shore frequent different kinds of bottom, doubtless in search of their food; and different portions of
our Atlantic bays are known as “haddock ground,” and “cod ground,” the former always being caught on sandy bottom,
while the cod frequent stony and rocky bottoms. These facts may very well explain why one part of a geological forma-
tion may abound in certain forms, while another, varying somewhat in character, may contain a very different congregation
of fossils. *
The lithological character of rocks, therefore, is an element to be taken into consideration when we undertake to identify
strata by their contained fossils. - -
HAMILTON GROUP. 187
The valleys of Seneca and Cayuga lakes are both excavated, for more than half their length,
in the shales of this group; and the banks of these lakes, with the lateral ravines, afford the
best facilities for examination. The group appears also to be better developed in this part of
the State than farther west, there being in that direction a gradual thinning of the different
Iſla SS6S, \ - - . .
Along the banks of these lakes I have been able to trace the following subdivisions, which
hold good over considerable areas, but which cannot be relied on in every instance; for to-
ward the western extremity of the State some portions are lost or merge into others, so that
the same lines of subdivision cannot be recognized. These divisions, which have been enu-
merated in the annual reports, are the following: - ,
1. Dark, slaty fossiliferous shale, which rests directly upon the Marcellus shale, there
being, as before remarked, no very well defined line of separation between the two. This
part of the group is not very abundant in fossils; it may be seen in the towns of Warick and
Fayette in Seneca county, and on Flint creek and Mud creek in Ontario county.
2. A compact calcareous blue shale, often passing into an impure limestone. The mass is
quite thin, and worthy of notice only from being somewhat persistent, and marking the point
of separation between two more important shaly masses. This is visible on the banks of
Cayuga and Seneca lakes, on Flint Creek, and was traced as far as the west side of the Ge-
nesee river. -
3. An olive, or often bluish fissile shale rests upon the last named mass. It is marked by
small concretions, and contains a few Cyathophylli and some other fossils. Toward the upper
part, this shale becomes very fissile and of an olive color, often stained by oxide of manganese.
It can be seen on the shores of both the lakes just mentioned. -
4. Ludlowville shales. The latter mass passes by insensible gradation to a more compact
rock, which contains an admixture of sand, and often separates in large masses which resist
the action of the weather for a long time. Above this part the rock is a soft bluish grey shale,
which is more calcareous and fissile, and contains a different association of fossils. These two
kinds, with the next below and the two above, appear at and near the village of Ludlowville,
in Cayuga county; and since these rocks are of the same age as those of the Ludlow forma-
tion of England, described by Mr. Murchison, this is a desirable locality to perpetuate the
Ila.IY16. - - -
5. Encrinal limestone. This rock is a thin bed, usually of impure limestone, with a great
abundance of crinoidal columns. Sometimes the mass is a compact shale, held together by
columns of great size and length. It is a persistent mass, holding only one position in the
group, and continuous as far as Lake Erie. It is a convenient point of reference, and will be
frequently mentioned in the description. It rests upon the last named shale, separating it
from the Moscow shale. * }
6. Moscow shale. This mass succeeds the encrinal limestone, and is a well defined and
persistent mass throughout the district. It is of a greyish blue color, and scarcely laminated;
it separates into irregular fragments, which are rarely slaty. It is slightly calcareous, and
abounds with fossils, many of them unlike those below. tº -
24*
188 GEOLOGY OF THE FOURTH DISTRICT.
With this mass terminates both the peculiar shales of which the group is composed, and
also the greater part of those fossils typical of the same, so far as regards the Fourth District.
The divisions here enumerated may be found of service to the careful observer, and they
afford some interesting facts regarding changes in fossils; still they cannot all be described
as distinct, neither is it of practical importance that they should be.
From the fact that the position of the last is well marked, being embraced between the
Encrinal limestone below and the Tully limestone above, and also containing a peculiar asso-
ciation of fossils, it is everywhere recognizable, and as a subdivision is more important than
some of the others. - -
The subdivisons here enumerated can all be seen on the eastern shore of Cayuga lake, be-
tween Springport and Ludlowville; the latter place also presents the two next higher rocks of
the system.* The eastern shore of Seneca lake exhibits the same between its outlet and
Lodi, in Seneca county. The same rocks appear, but not so well exposed, on the western
shores of both lakes. This fact is of interest, as showing the influence of the prevalent
westerly winds, which, from the constant action of the water driving against the eastern
shores, has undermined the mass, and a perpendicular cliff is thus constantly kept exposed.
The operation of the same cause has produced a fine exhibition of the rocks of this group
upon the shores of Lake Erie. w
This group of rocks occupies a belt of country from five to eight miles wide, extending
through the counties of Seneca, Ontario, Livingston, Genesee and Erie.
In the county of Seneca it occupies the southern part of Fayette, the whole of Varick,
nearly the whole of Romulus, and that portion of Ovid bordering the shores of both lakes.
The superior rocks have been greatly denuded, and the surface of the group is greater than
in any part of the country westward. Its southern limit, which is just north of the village of
Ovid, is several miles farther south than any other point before coming to Lake Erie. The
two lakes, Seneca and Cayuga, seem to have been the great outlet of northern waters, and
along their channels the great excavating and transporting force seems to have operated with
peculiar energy. - -
On the eastern side of Seneca lake the group is well exposed in the outlet of Crooked lake,
which in its passage to Seneca lake has excavated a channel from rocks of the Portage group,
through the Genesee slate, the Tully limestone and Moscow shale, exposing the two latter to
great advantage, and presenting localities where great numbers of the finest fossils can be
obtained. The illustration at the head of this group presents a conical hill of the Moscow
shale, succeeded near the top by the Tully limestone, and above this a thin band of Genesee
slate, upon which is a covering of alluvium. The sloping hills on either side are indented
by numerous ravines which expose the rocks of the same group. It also occupies the eastern
margins of the towns of Benton and Milo in Yates county. l -
In Ontario the group occupies nearly the whole of the town of Seneca, the southwestern
part of Phelps, the northern part of Gorham, nearly all of Hopewell, the whole of Canandai-
gua, East and West-Bloomfield and Lima.
ºrssm-
* See Section, Plate VII.
HAMILTON GROUP. 189
In these towns there are numerous good exposures of the group, the best of which are
along Canandaigua lake and in the ravines upon either side. The banks of Flint creek also
afford a good opportunity of examining the whole series, and the several subdivisions as enu-
merated may be found between Vienna and the village of Bethel, where the Tully limestone
and Genesee slate succeed this group. On the north of the turnpike from Geneva to Canan-
daigua, there are several ravines which disclose these shales in great perfection. The parts
of the group here exhibited are principally the encrinal limestone and the shales below, which
abound in fossils. The upper part of the division, denominated Ludlowville shales, is well
marked by great numbers of Delthyris mucronatus and Atrypa concentrica, with one or two
species of Strophomena; the lower part contains large numbers of Cypricardia and Avicula,
and is more sandy in character than that above. The same portion of the mass is also well
developed on Canandaigua lake, where its fossils are numerous. The lower part of the group
is also seen, as well as the Moscow shale above.
In Livingston county this formation occupies nearly the whole of the towns of Avon and
York, a part of Geneseo, Leicester and Caledonia. The deep valley of the Genesee, with
numerous lateral ravines and water courses, renders this county one of the most desirable loca-
lities for examining the rocks of this group. The Moscow shale receives its name from the
beautiful development of the same on Beard's creek, on the land of Mr. Horsford; and it con-
tains at this locality more than fifty species of fossils, many of which do not occur in any part
of the group below. The rock at this place is a pure calcareous mudstone, of a bluish color
on first exposure, but weathering to a whitish ashen. Its decomposition is hastened by the
diffusion of iron pyrites, which sometimes replaces the fossil bodies. At this locality the
Genesee slate succeeds, without the intervention of any other rock. Several miles north
of this point, on the land of the Hon. G. W. Patterson, the shale is well developed in a small
ravine, and also at one or two other places in the immediate neighborhood.
About three fourths of a mile west of York centre, there is a fine development of the shale
immediately below the encrinal limestone. The latter also appears here in the form of a shaly
limestone, with numerous crinoidal stems and other fossils. The shale is completely charged
with Cyathophylli of different species, Favosites and other corals, with some trilobites and
shells. In following down this ravine towards the river, the lower divisions of the shale are
but obscurely seen, till we arrive at the thin division, before mentioned as the calcareous blue
shale (or shaly limestone), which at this place is compact, and a tolerably pure limestone.
On the east side of the river, at Jacock's run, the Moscow shale, Encrinal limestone, and
the higher part of the Ludlowville shales, are well exposed, and offer an abundance of fine
fossils, among which are several beautiful corals of the genus Retepora or Fenestella. By
following this ravine towards the river, the lower division of the group may be seen. At an-
other ravine a mile or two farther south, the same shales are exhibited in a good degree of
perfection. w
The Moscow shale is seen near the base of the fall on Fall brook, south of Geneseo village.
The same is also seen near the Conesus outlet, and along that stream the lower divisions of
the group are well exposed at several places. '^
190 - GEOLOGY OF THE FOURTH DISTRICT.
The lower divisions of the group are seen in Allen's creek, south of Le Roy; and the
higher portions, with the Moscow shale, at Pavilion and Bethany. A little distance to the east
and south of Batavia, the lower part of the group is well exposed, and in Alexandria the higher
divisions of the same. - e
In the town of Darien, a little west of the Centre, there is a good exposure of the upper
part of the Ludlowville division and the Encrinal limestone; the latter is a compact mass
about three feet thick, and its upper part strongly stained from decomposing iron pyrites.
The shale abounds with Atrypa affinis, A. concentrica, Delthyris mucronatus, and other spe-
cies of these genera. Cyathophylli, Strombodes, Favosites, and other corals are almost as
abundant as at York in Livingston county. The Moscow shale is tolerably well exposed at
this place, though its decomposition upon the surface has obscured its characters, and it pre-
sents the appearance of an ordinary clay bank.
On the road westward from the last named place, the rocks of the group are exposed in
several places. On a small stream crossing the road near Alden, the shales are well exposed;
and a little south of this, the encrinal limestone is quarried. It is here highly fossiliferous;
containing, in addition to the usual abundance of crinoidal columns, Delthyris, Pleurotomaria,
and Calymene bufo. At this and many other localities, this thin calcareous mass appears to
be a common depository of many or all the species of the shale below, with several others
which are peculiar to itself. It was of course produced during a cessation of the mud deposit;
and the forms living on the bed of the latter would consequently be inclosed in this deposition,
with others produced on the calcareous bottom, some of which are different.
Along the Cayuga Creek, on the Indian reservation, these shales can be traced from near
their base, throughout, to their connexion with the higher rocks. And here I should not omit
to state what has appeared, only more indistinctly, at other localities. The division noticed
as the olive shale, and the band of blue calcareous shale, with the sandy part of the Ludlow-
ville division, have, almost or entirely, disappeared, apparently from a gradual diminution in
the quantity of matter. The gradual thinning becomes very apparent at all the localities
west of the Genesee river. At the same time all those portions which are persistent, except
the encrinal limestone, have diminished in the same direction; and although few localities offer
good exposures, it is, nevertheless, very evident that such is the fact.
This becomes more palpable when we arrive at the shore of Lake Erie, which offers
the best continuous exposure west of Seneca lake. It is here quite evident that the rocks
have diminished to less than one half the thickness which they have on Seneca lake. At the
same time, however, many of the fossils have maintained their position, and some species
seem even to be more abundant than eastward. The Cypricardia, Avicula, Nucula, Belle-
rophon, and a few others appear to have diminished in numbers according to the diminution
of the sandy calcareous shale in which they so abound at the east. - -
To show, however, how fixed are their habits and place of residence, there is a stratum of
this kind on Lake Erie, which is indicated by the letter a, in the section Plate 5, in which
Cypricardia, Turbo, Bellerophon and Orthoceras occur to the almost entire exclusion of eyery
thing else. This stratum, too, holds the place which the thick mass of similar character does
HAMILTON GROUP. I91
further east; and directly above it we find bluish calcareous shales, with Delthyris mucronata,
Atrypa concentrica and A. affinis, being the characteristics of the upper part of the Ludlow-
ville division of this group. -
This fact is sufficient to show that there were distinct periods of formation, and that the
thick mass of sandy shale so abounding in the conchiferous mollusca in the eastern part of
the State, and which in the central part is still in great force, extended westward entirely to
lake Erie. It is there recognized by the same lithological characters, the same or a similar
association of fossils, and holds the identical place in the strata.
The section of this group on Lake Erie (see Plate 5) commences with the shale immedi-
ately above the Marcellus, and from thence the continuation is nearly unbroken throughout.
The characters of the lower and higher divisions are more nearly alike than farther east, the
whole being a soft bluish shale, readily crumbling on exposure to the atmosphere, and decom-
posing to a tenacious mud. The sandy portion is scarcely noticed, and thin beds of black
slaty shale, so common on Seneca lake and other localities in the central part of the State,
have entirely ceased. The peculiar fossils of these portions are likewise wanting, showing
the association of certain forms with products of similar nature. The fossils here alluded to
are a species of Orbicula, the Atrypa congregata of Conrad, and some others. -
Notwithstanding that fossils are exceedingly numerous in this exposure along Lake Erie,
it must be acknowledged that there is a manifest decrease in the number of species. Scarcely
any new ones are noticed, and many which have been common at the east are rare or wanting.
There are several species which abound in immense numbers, and which in this respect fully
compensate in number of individuals for the absence of a larger number of species. This
fact of the gradual disappearance of fossils is equally obvious with the decreasing thickness
of rocks which is observed as we progress westward. Whether this was caused by increased
depth of water, distance from shore, or by the thinning of the deposit alone, it may be inte-
resting to inquire; probably, however, all these causes operated in some degree to produce
the result. -
The lower divisions of this group on Lake Erie, or that part below the stratum marked a
in the section, are nearly destitute of fossils, and the forms which seem peculiar to this part
on Seneca and Cayuga lakes are not found here. The three upper divisions are here the
only ones which are interesting from their organic contents.
Throughout the whole period of this deposition, there appears no evidence of any distur-
bances. The character of the materials, the condition of the fossils, all show the absence of
violent currents or of powerful waves. The deposit was probably made at a depth below
water, beyond the reach of the waves which may have agitated the surface; and there ap-
pear to have been no oscillations by which one portion of its extent was elevated, while
another was depressed. It was emphatically a long period of repose.
192 GEOLOGY OF THE FOURTH DISTRICT.
Joints or Vertical Cleavage.
The rocks of this group, where exposed in cliffs or in the banks of ravines, are traversed by
numerous joints, usually vertical to the planes of stratification, but sometimes slightly oblique,
and again more or less curved. These will be more fully described in the chapter relating
to that subject alone. The following sketch exhibits the appearance of a natural section of
the Moscow shale on the banks of Cayuga lake. * ,
Jointed structure of the Cliffs on Cayuga lake. From a sketch by Mr. E. N. HoRSFORD.
It will be seen that these joints do not all continue through the part of the mass exposed,
but the blocks exhibit a series of steps which limit the depth to which these divisional
planes extend. This structure is very favorable to the rapid abrasion and undermining of
the cliffs along the lake shore. The water finds access to the slightly opened fissures, which,
in the colder seasons, are enlarged by the freezing of the same, and in summer the waves
dash into them, constantly widening the breach. A slight undermining causes a separation
by the joints in the opposite direction, and the waves in time leave them standing in isolated
blocks, which are gradually undermined, and fall into the lake. Examples of this kind are
frequently seen, not only in this group, but in those next succeeding, and more especially the
Portage group, where they are illustrated. .
Concretions or Septaria.-These bodies, presenting various fantastic forms, are of frequent
occurrence in this group, though not so abundant as in the shales below and above. Many
of them, as before noticed, are calcareous concretions, which appear to have aggregated
around a fossil body or a small nodule of iron pyrites. In the latter case the mass usually con-
tains pyrites, and it is probably owing to the attractive force of this substance that they were
produced. Fossil shells are frequently found in the centre of these bodies, and the outer
surface is often covered with them,
HAMILTON GROUP. - 193
Nodules of iron pyrites, often embracing a fossil in the centre, are
of frequent occurrence; they are usually uninteresting, except as
showing the incipient stages of this process. The small figure in the
margin represents one of these aggregated around a Lowonema, a
portion of which projects above.
The septaria are spherical, flattened or oblong, and crossed by numerous seams of calcare-
ous spar, and in the centre is frequently a cavity lined with crystals and partially filled with
fluid bitumen. The figure below represents a small specimen of this kind from the shore of
Lake Erie. It is figured for the purpose of illustrating the general appearance of these bodies,
which are frequently taken for some fossil.” The calcareous concretion is first formed, and
afterwards cracks, and the spaces become filled with crystalline matter from segregation or
infiltration. Sometimes there are no cracks in them, and at others these are filled with clay
or shale.
º
M£%
<3Hº
\
s$
|
Nº
Q
\
|
Nº.
º
}
;
Localities—The description of this group has necessarily led to the mention of many loca-
lities; but as the object of this head is to direct observers to the most important points, I may
mention the banks of Cayuga and Seneca lakes, the ravines on the Genesee river, in Avon,
# The common belief is that these bodies are petrified tortoises or turtles, and that the seams are the divisions of the
plates of the shell. So firm is this belief with many persons that they are kept as an evidence of former living animals,
while the multitudes of shells in the saue rock are entirely overlooked. -
[GEOL. 4th DIST.] - 25
194 GEOLOGY OF THE FOURTH DISTRICT.
York and Leicester, and the shore of Lake Erie at Eighteen-mile creek, as the most impor-
tant and interesting points, and which will give all the desired information of this group in the
Fourth District. 3 .
Thickness. – The thickness of this group on the eastern limit of the district cannot be less
than 1000 feet. There are a few undulations in the strata which may mislead in the esti-
mation, to a small extent. Each of the members noticed thins gradually toward the west,
until on Lake Erie it is less than half that amount. The whole thickness visible at this point
is about one hundred feet. The Moscow shale, which in the eastern part of the district is
fifty or sixty feet thick, is on Lake Erie 15 feet thick, and the lower members have diminish-
ed in equal proportion; the shale of Ludlowville, known by the great numbers of Avicula,
Cypricardia, &c. is scarcely a foot thick in the west. *
Mineral contents of the rock. —From the nature of the rock, and the absence of all distur-
bances and intrusive rocks, it will be presumed that there are few simple minerals. Those
which do occur are usually in the concretions; crystallized carbonate of lime and baryta, and
sometimes blende and galena occur in these bodies. Iron pyrites occurs in all situations, and
from its decomposition result sulphate of alumina and sulphate of iron.
The presence of blende, galena and other minerals proves that, under more favorable cir-
cumstances, these rocks might have been somewhat metalliferous; but being, in its present
state, an unaltered mechanical deposit, the substances of this kind which it contains are dis-
seminated through the mass, and the quantity is so minute as to be unappreciable while so
diffused. .
Springs.--From the generally impervious nature of the rocks composing this group, it
gives origin to numerous springs which rise to the surface in all situations. Wherever the soil
is thin above the rock, the place is manifested by a wet or damp soil; and though there are
few prominent and important springs, yet the water is carried to the surface, and oozes out
over large spaces. Water is easily procured by digging wells in all situations where this rock
underlies the surface, unless it be too deeply covered with alluvion. This is the condition in
some parts of Bloomfield, Ontario county, where the rock has been deeply excavated, and
the space afterwards filled with an immense deposit of northern drift, which rises into innume-
rable hills and long ridges. From the great number of low conical hills clustered together in
these situations, they are known by the name of the “Hopper hills.”
Agricultural characters of the group.
The soil resulting from the decomposition of these rocks, when unmixed with foreign ma-
terials, varies from a tolerably pure marly clay to clayey loam; but the prevalence of northern
drift over a large part of the surface occupied by this group, has essentially modified the cha-
racters of the soil covering it. The sandy calcareous portion of the shale has given origin to
a clayey loam, which, in some places in the eastern part of the district, remains nearly un-
HAMILTON GROUP. I95
mixed with foreign materials. The soil varies, however, from a stiff clay to sandy or gravelly;
and sometimes these divisions are arranged over considerable areas, apparently without refe-
rence to the rocks beneath. º
As an example, we find, in passing over this group from Seneca lake westward, that there
are alternations of sandy, gravelly and clayey soils, as far as the valley of Flint creek; passing
this, the soil is for the most part Sandy and gravelly, passing into a gravelly clay, till we reach
the summit between Flint creek and Canandaigua lake; and descending from this point to the
outlet of the lake, the soil is almost wholly clay. Again, on the west of this lake the soil is
clay or clayey gravel, till we arrive in Bloomfield, where it varies from a light sandy loam to
gravel and gravelly loam, with but little clay except in the low grounds.
Farther west, and particularly in the valleys, the soil is more clayey where this group
extends. Approaching Lake Erie, the northern drift has accumulated above these rocks, and
the soil presents a gravelly and loamy character, with occasional tracts of clay in low grounds,
or in places where the rock approaches the surface. Along the shore of Lake Erie, where
this group extends, there being no considerable proportion of drift, the soil is extremely clayey,
as any one may recollect who has travelled the road southwest from Buffalo in the wet season.
Whatever kind of soil prevails, however, it is always highly calcareous, and over the whole
extent of the group is of unequalled fertility. A large proportion of the famous “Genesee
country” lies upon this group, and the fertility of this soil is well known. The materials de-
rived from the destruction of the rocks of this group are largely intermingled with the soils to
the south of their southern boundary, and contribute largely to the fertility of the slopes under-
laid by rocks of the Portage group, and the broad valleys which extend southward nearly to
the Pennsylvania line.
Organic Remains of the Hamilton Group.
The contrast in the prevailing fossils of this group with those of the last is as great as in
the lithological products of the two formations. We sometimes indeed meet with a species
which occurs in the limestone below, but except in a few instances these recognitions are rare.
Some of the more abundant corals are identical, but the great number of new forms renders
them of less importance, and in all instances they are too few in number to produce any doubt
or difficulty in identification of strata. - -
Shells both of the Brachiopoda and Dimyaira have immensely increased, and in many single
localities from twenty to fifty species of fossils may be obtained. The great abundance and
perfection of these fossils offer strong inducements for the study of this branch, and perhaps
no other department of Natural History, except Botany, will yield so rich a harvest from
limited areas as Palaeontology. If their occurrence in the lower rocks, as represented in this
volume, is interesting, their great number and exquisite perfection in the Hamilton group will
certainly delight the mind of every lover of Nature. Here it seems, that instead of extract-
ing them from the solid rock, we are culling them from the dried ocean mud, which a late
25*
196 GEOLOGY OF THE FOURTH DISTRICT.
retiring sea has left above its reach, so much do these soft shales resemble the mud deposits
on the bays and creeks along the sea shore.
The following woodcuts are illustrations of the prevailing forms in different parts of the
group. Those from the lowest portions are omitted.
1. Bellerophon patulus. 4. Nucula oblonga, 7. Nucula bellatula.
2. Microdon bellastriata. 5. Nucula lineata. 8. Cypricardia truncata.
3. Cucullea opima, 6. Tellina? ovata. 9. Modiola concentrica.
1. Bellerophon patulus, n. S. — Sides slightly umbilicated, aperture suddenly and broadly
dilated, nearly smooth, or with faint undulating striae, which become stronger and slightly
arched in receding from the margin. *
The striae become very strong and sharply arched upon the first volution.
Locality — Cayuga lake shore. -
2. Microdon bellastriata (CoNRAD, Jour. Acad. Nat. Sci. Vol. 8, p. 247, pl. 13, fig. 12).-
Compressed, broadly oval and somewhat truncated posteriorly; marked by numerous equal
concentric striae. -
This is a beautiful and easily recognized shell. It is often abundant in the harder shales,
but in the western part of the district is exceedingly rare. It is one of those fossils having a
wide geographical range, being known in the middle and southwestern parts of Virginia.
The young of this shell closely resembles the figure of Venus parallela (PHIL. Geol.
Yorkshire, Part il, pl. 5, fig. 8).
Locality—Banks of Seneca and Cayuga lake; Crooked lake outlet; more rarely in the
Genesee valley. -
HAMILTON GROUP, I97
3. Cuculled opima, n. S. – Ovate, very convex; beaks near the anterior extremity, very
prominent; surface marked by strong concentric lines; cast nearly smooth; impression of
the internal laminae oblique. *.
When compressed, this fossil has the appearance of a Nucula; but the impressions of the
internal laminae seem sufficient to warrant its reference to Cucullea.
Locality—Ovid, Seneca county.
4. Nucula? oblonga.-Oblong, elliptical, very inequilateral, very finely and concentrically
striated; an impressed line extends from the hinge, just forward of the beak, half way to the
base. - .
This is a very common form in the eastern part of the district. -
Localities—Cayuga and Seneca lake; Outlet of Crooked lake; Genesee valley.
5. Nucula lineata? (PHILLIPs, Paleozoic Fossils, p. 39, fig. 64).-Sub-triangular, con-
vex; beaks much elevated; surface covered with coarse concentric striae. -
This shell is not very uncommon in the ravines about Seneca and Cayuga lakes, though the
specimens usually seen are much compressed and distorted.
Locality—Seneca lake shore; Shelldrake point on Cayuga lake.
6. Tellina? ovata, n. S.–General form ovate, produced posteriorly, and apparently slight-
ly gaping at the extremity; posterior slope angulated; surface covered by minute concentric
striae, which become more prominent near the margin.
Since no teeth are visible in the hinge line, and the external form is so analogous to Tellina,
it is referred to that genus.
Locality—Cayuga lake.
7. Nucula bellatula, m. s. – Ovate, somewhat contracted near the posterior extremity;
surface covered with regular, fine concentric striae; teeth in the hinge margin very distinct.
There is a slight depression extending along the posterior slope, giving a contracted appearance
to this part of the shell. -
This beautiful little shell is often seen in the harder shales of the group.
Localities—Cayuga and Seneca lakes.
8. Cypricardia truncata. (Cypricardites truncata, CoNRAD, Jour. Acad. Nat. Sci, Vol.
8, p. 244, pl. 12, fig. 17.)—Trapezoidal; surface covered with concentric wrinkles; pos-
terior slope sharply carinated. The wrinkles upon the posterior slope are parallel to the
truncated margin, and nearly at right angles with those upon the side of the shell.
Compare Cuculled arguta (PHIL. Geol. Yorkshire, Part ii, pl. 5, fig. 20).
Locality–Cayuga lake. -
9. Modiola concentrica. — Oblong-ovate, very inequilateral; surface covered with regular,
equal concentric striae, which become confluent towards the base; hinge line curved; anterior
side short, with a longitudinal impression directly below the beaks. -
198 GEOLOGY OF THE FOURTH DISTRICT.
This is a very abundant fossil, being found in the coarser shales over all the eastern part of
the district. It resembles the figure of Modiola? semisulcata (Silurian Researches, pl. 8,
fig. 6). & . *
Localities—Cayuga and Seneca lakes; Outlet of Crooked lake; Ontario and Livingston
COllníI€S.
79.
§
% º
is
º §
*
|
º
%%ill. *N :
% %iºs
% | § W §§
*†.
ºliº
§iº
lińº
1. Turbo lineatus. 2 and 3. Delthyris mucronata. 4. Atrypa prisca. 5. Atrypa concentrica.
1. Turbo lineatus, n.s. – Turbinate, obtuse; surface marked by several sharp spiral lines,
all which, except the central one, are not visible on the cast; longitudinally striated; last whorl
of the shell rapidly expanding; aperture orbicular; umbilicus moderate.
This fossil occurs generally as a cast, and in some places is abundant, frequently invested
with a coral.
Locality—Ovid, Seneca lake shore.
2 and 3. Delthyris mucronata (Annual Reports of the New-York Geological Survey, 1841,
p. 54). —Varying in form from semicircular to triangular, with the hinge line greatly ex-
tended; surface marked by 24 to 30 rounded ribs, which are crossed by crowded undulating
elevated lamellae, giving a squamous appearance to the shell; hinge area very narrow ; aper-
ture small. Figure 2 is the nearly semicircular form; fig. 3 shows the hinge line more ex-
tended; and fig. 3 of Illustration 84, presents a still more extended hinge line, from the shaly
sandstone of the Third District. . - - • ‘
This is a very ornamental shell, and its numerous varieties in form are very interesting.
In the soft calcareous shales of western New-York, it is shorter and more rotund; while in
the sandy shales and shaly sandstones of the middle and eastern part of the State, it is greatly
extended, and its extremities very acute. Occurs in all localities of the upper middle portion
of the group.
HAMILTON GROUP. I99
4. Atrypa prisca. (Terebratula affinis, Min. Con. ; T. prisca, Von BUCH; T. reticularis,
BRONN, Lethea Geog. ; Atrypa reticularis, DALMAN: A. affinis, Silurian Researches.)—
Oblong, often nearly circular; lower valve least convex, with the beak scarcely prominent,
and pressed close to the beak of the upper valve; upper valve very convex; front margin
often advanced and a little depressed; surface radiated with numerous round striae, which
bifurcate at irregular intervals.
The specimens vary in size, and very frequently are flattened from compression, so that
they do not present the rotund form of the figure. This is an abundant and widely distri-
buted fossil, appearing throughout the Hamilton and Chemung groups. It is more abundant
in the Hamilton group just below the Encrinal limestone, associated with the preceding and
succeeding forms. It also occurs in the Moscow shale in great numbers.
Localities—Seneca lake; Hopeton; Moscow; York; Darien; Eighteen-mile creek, &c.
5. Atrypa concentrica (BRONN, Lethea Geog.).--Spheroidal, flattened or rotund, impress-
ed in front; upper valve very convex in the middle, slightly elevated in front and depressed
at the sides; beak scarcely prominent, and closely pressed to the beak of the lower valve;
lower valve convex, with a prominent, slightly incurved beak, and a mesial sinus extending
two-thirds the length of the shell, elevating the front; surface marked by numerous concentric
striae, which in young specimens are projecting lamellae, giving the shell a squamose ap-
pearance.
This is an exceedingly abundant fossil in many places, and appears in the greatest num-
bers just below the Encrinal limestone. Sometimes it occurs in the shale above this stratum,
associated with Orthis umbonata. It will be readily recognized from its general smoothness
and numerous concentric lines. -
Localities—Seneca and Cayuga lakes; Hopewell; Conesus outlet; Darien; and in greater
numbers and perfection at Eighteen-mile creek on Lake Erie.
200 GEOLOGY OF THE FOURTH DISTRICT.
The following illustration presents some of the typical fossils of the Moscow shale. Seve-
ral of these have not been seen in the group below while others do occur in lower situations.
80.
- A. -
º º S
1, 1 a, 1b, 2. Atrypa spinosa. 5. Delthyris ZigZag.
3. Atrypa concinna. - 6. Calymene bufo.
4. Strophomena inequistriata.
7. Cryphaeus calliteles.
8. Loxonema sinuosa.
1 & 2. Atrypa spinosa, n.s.—Sub-orbicular, often flattened, producing an angle at the extre-
mities of the hinge; beak of the lower valve slightly prominent, incurved; surface with about
twenty rounded radii, which bifurcate often very regularly at less than half the distance from
beak to base; radii crossed by numerous elevated lamellae, which upon each rib are folded
and extended into a spine of one-fourth to one half an inch in length; surface between the
lamellae concentrically striated. -
The shell more commonly appears without the spines, or with them partially worn off.
When destitute of spines, it resembles the figure of A. squamosa (SowHRBy, Geol. Trans.
2d series, Vol. 5, pl. 57, fig. 1).
Fig. 1 is of a specimen from Eighteen-mile creek, where the spines are always absent.
Fig. 2 is of a specimen from Moscow, where the spines are more or less perfect, being en-
cased around the margin in soft shale, and worn off on the prominent part of the shell.
This fossil is frequently confounded with Atrypa prisca.
Localities—Moscow, Eighteen-mile Creek.
3. Atrypa concinna, n. S.–Lenticular, nearly smooth, or with a few distant elevated lines
of growth; lower valve most convex, with a faintly impressed line extending from beak to
base; beak of the upper valve scaréely prominent, and closely pressed within the lower one;
beak of lower valve prominent, small, acute, incurved.
HAMILTON GROUP. 201
This is a very glabrous shell, with a prominent line of growth near the beaks, and one or
two more near the margin, leaving the greater part of its area entirely plain.
Localities—Moscow, Eighteen-mile creek. -
4. Strophomena inequistriata (CoNRAD, Jour. Acad. Nat. Sci. Vol. 8, p. 254, pl. 14,
fig. 2). — Somewhat semicircular; lower valve very convex; surface covered with radiating
striae, every fourth or fifth of which is more prominent than the rest; striae increasing in
number towards the margin; hinge extremities angulated. -
There seems to me very good reason for considering this form and the S. mucronata (CoN-
RAD, Jour. Acad. Nat. Sci. Vol. 8, pl. 14, fig. 10), as identical, and that both are identical
with Orthis interstrialis (PHIL. Palaeozoic Fossils, p. 61, pl. 25, fig. 103, a, b, c, d ).
In the calcareous shales of the Hamilton group, its form is often better defined and more
rotund, though the striae are less sharp ; while in the Chemung rocks, it is usually compressed,
and very frequently the shell is partially or entirely removed.
Locality–Seneca lake; Moscow.
5. Delthyris zigzag, n.s.- Upper valve semicircular, moderately convex; surface marked
by 16 to twenty rounded ribs, which are crossed by very prominent undulating or zigzag la-
minae; mesial fold of the upper valve somewhat duplicate, of the lower valve deeply impressed
and elevated in front. º $
So far as known, this fossil is confined to the Moscow shale. It is readily distinguished by
the prominent zigzag laminae. & -
6. Calymene bufo (GREEN, Monograph, p. 41). — Head semicircular; middle lobe very
large, obtuse in front; surface covered with numerous depressed pimples; articulations of the
body 10, of the tail 8; articulations of the middle lobe apparently double, those of the lateral
lobe deeply grooved near their junction with the central lobe.
The fossil from which the drawing is taken is partially coiled, so that the tail is not visible.
It is one of the most abundant fossils of the group, occurring either perfect or in fragments at
nearly every locality.
Localities—Moscow; Seneca lake, and Eighteen-mile creek.
7. Cryphaus calliteles, GREEN.—Head lunate, with the posterior angles of the buckler
extended to the fifth rib of the body. Articulations of the abdomen 10; of the tail, 10 in the
middle, and 6 in the lateral lobes. Articulations of the lateral lobes free at the margin, and
forming a beautiful punctulated fringe. Structure of the head and eyes like the Asaphus.
Surface pimpled, and, apparently from the removal of these, punctulated.
Localities—Moscow; Pavilion; Eighteen-mile creek.
8. Loa onema neasilis (PHIL. Palacozoic Fossils, p. 99, pl. 38, fig. 183. Terebra nearilis,
Sow ERBy, Geol. Trans. 2d Series, Vol. v., pl. 54, fig. 17.)— Elongated, subulate; volutions
convex, with alternating longitudinal arched furrows and raised lines, retiring from and ad-
vancing toward the sutural lines. (The specimen figured is imperfect.)
[GEOL, 4th DIST.] 26
202 GEOLOGY OF THE FOURTH DISTRICT,
The raised lines are less arched than in L. sinuosa (Terebra sinuosa, Silurian Researches,
pl. 8, fig. 15), which also occurs in this group, and are almost straight on some of the higher
whorls. -
Locality—Seneca lake; Moscow.
The specimens figured in the following illustrations appear to be confined to the thin band
of Encrinal limestone below the Moscow shale.
81.
1. Avicula orbiculata. 2. Atrypa rostrata. 3. Atrypa. 4. Atrypa. 5. Atrypa. 6. Delthyris.
1. Avicula orbiculata, n. S.–Roundish, auriculated; slightly oblique hinge line shorter
than the width of the shell; posterior wing extending nearly in a line with the margin of the
shell. Surface covered with rounded radiating ribs, which become fainter upon the upper
lateral margins; these are crossed by rounded concentric lines, which are less prominent than
the others.
The nearly round figure of this shell forms a prominent feature of its distinctive character.
Locality—Eighteen-mile creek.
2. Atrypa rostrata, n. S. – Obovate ; valves nearly equally convex, lower one with a lon-
gitudinal depression from beak to base; beak of the upper valve scarcely prominent, of the
lower valve very prominent, produced and incurved over the upper one. *
This is a very neat little shell, marked by a few concentric lines of growth.
Locality—Eighteen-mile creek.
, n. S. – Elliptical, slightly elongated at the beak; valves nearly equally
convex, smooth, or with faint concentric lines of growth; beak of the lower valve prominent,
rather small, and slightly incurved.
This shell is larger than the last, the beak smaller proportionally, and less incurved, and
there is no depression on the lower valve.
Locality—Eighteen-mile creek.
3. Atrypa
HAMILTON GROUP. 203
4. Atrypa . — Obtusely cuneate ; valves equally convex, with about 16 plicae on each,
three of which are raised in front; beak of the lower valve prominent, small, that of the upper
closely pressed to the lower.
This shell often varies in size from the figure.
Locality—Eighteen-mile creek.
5. Atrypa , n. s. – Broadly obovate, tapering abruptly to the beak, and rounded be-
low ; lower valve most convex; beak of the lower valve large, very slightly incurved; that of
the upper valve small, rather prominent, and closely pressed to the lower valve.
This shell is distinguished from figs, 2 and 3, by its broadly rounded base, the large, pro-
minent, nearly straight beak of the lower valve, and the slight radiating elevated lines which
are visible in the cast. a
Locality—Eighteen-mile creek.
6. Delthyris sculptilis, n. s.—Semicircular, somewhat auriculate; surface marked with
eight prominent ribs, which are crossed by strong elevated laminae of growth, the spaces be-
tween which appear as if grooved; the mesial elevation of the upper valve scarcely larger
than the ribs. - -
At first view this fossil appears much like the D. zigzag, but there are fewer ribs, and the
laminae are more deeply sculptured. So far as known, this fossil is confined to the Encrinal
limestone. -
Locality—Eighteen-mile creek.
The following species of Avicula is associated with the Encrinal limestone of this group
throughout the district.
82,
*
|
1 and 2. Avicula decussata.
1 and 2. Avicula decussata, n. S. – Obliquely ovate or sub-rhomboidal; surface marked
by numerous fine radiating lines, which are decussated by irregular concentric lines of growth:
the concentric lines are rather like wrinkles, and stronger than the radiating lines.
26*
204 GEOLOGY OF THE FOURTH DISTRICT.
Fig. 1 is a cast in limestone, in which only the concentric lines are visible. In fig. 2, the
shell is still retained, and presents the two series of lines. This is from the limestone where
largely intermixed with shale. - - . .
Localities—York; Darien; Alden; Eighteen-mile creek; Seneca lake; Outlet of Crooked
lake.
#
É
3.
3.
$3.ºº.*
3.
º
º
º%l
º
º
$:
āş
:
SS-
§
SS
§
Sº
§
%3.s
g§§
. sº
ºfflº,
| | º | º
º |}}}
º j
º
§
º
º
§
\
i
ſº
º {}
\},\!!!.
§§
W | Jºſh jº',
º
|
|
ºft
\ º º
§§ |
§§
}
º
N }; W
§§
The character of the Encrinal limestone of this group is well illustrated in the above wood-
cut. Fig. 1 is a small portion of the surface of a specimen of this limestone from Eighteen-
mile Creek. From being slightly weathered, the fragments of crinoidal columns, corals and
shells, stand out in relief. These fragments are sometimes invested with a coral, showing
that after their destruction they remained long enough upon the bottom for the coral to grow
and cover them. There are fragments of the columns of several species, of which no perfect
specimens have ever been found. Fig. 2 is a fragment of a large column, from the shaly
limestone in Livingston county. The pentapetalous canal has been filled with siliceous matter,
and the column around has decayed, leaving the former projecting for half an inch. Columns
of this size and larger are often found, of one or two feet in length; they are usually furnished
with branches, and these being broken off, they appear like knotty sticks.
The following illustration, from the Report of the Third District, presents some of the
characteristic fossils of this group in that part of the State, where it will be seen from previous
remarks that the lithological nature of the strata is somewhat different.
HAMILTON GROUP. 205
º
%
2 à Ea
% %
º º º Yº
%
% % Ø% Ø %2 %
º % Ż
*%
% ...”
%
%
%
1. Dipleura Dekayi. 2. Orthonata undulata. 3. Delthyris mucronata.
1. Head of Dipleura Dekayi (GREEN, Monograph, p. 79). — This portion of the fossil,
as well as the caudal extremity, are usually found detached, and in the sandy shales of the
Third District are abundant. In the softer shales of the Fourth District it is comparatively
rare, though I have seen it in many places. -
It ranges from the Marcellus shale throughout the group, and I have found the caudal ex-
tremity of a trilobite in the rocks of the Chemung group, apparently referable to the same
species. - -
2. Orthonata undulata (CoNRAD, Annual Reports). — This fossil is not unfrequent on the
eastern margin of the district, but far from presenting the perfectly delineated forms which it
does farther east. It entirely disappears before reaching the Genesee valley. -
This and the last named fossil, which are typical of the group in the eastern part of the
State, cannot be so considered throughout that portion west of Seneca lake.
3. Delthyris mucronata (CoNRAD, Annual Reports).-This is the common form of this
fossil in the sandy shales and shaly sandstones of the Third District; while, as we progress
westward into the soft calcareous mudstones of the group, its hinge line becomes less extended,
and the general form more rotund (see illustration, page 198 of this Report). It is one of the
most numerous forms, and appears almost equally abundant throughout the length of the State,
its maximum in the Fourth District being on the shore of Lake Erie.
The other forms figured on page 152 in the Report of the Third District, viz. Orthoceras
constrictum, Cypricardia recurva, Avicula flabella and Orbicula grandis, have all been seen
in the Fourth District, but they are not considered among the typical fossils of this group.
206 GEOLOGY OF THE FOURTH DISTRICT,
In addition to the fossils already presented from this group, we might introduce many more,
perhaps equally characteristic in different localities. The following among the Delthyris, may
serve to illustrate the prevailing forms of this genus.
1. Delthyris granulifera. — View of upper valve, presenting the duplicate mesial fold and
the granulated surface. -
1 a. End view of the same, showing the curved beak of the lower valve, and the spiral coil
within the shell. -
1 b. A specimen with a more extended hinge line. -
1 c, and 1 d. Two views of a smaller specimen of the same fossil.
This is by no means an uncommon fossil, though it is usually much compressed and dis-
torted, and the delicate points or granulations upon its surface are worn off. The specimen
fig, 1 is very free from compression, and presents the parts in true proportion to each other.
In fig. 1 b, the area is narrowed, from the upper valve having been pressed backward. The
fossil is very variable in the proportionate extension of the hinge line, sometimes being pro-
duced at the extremities into a point.
This specimen is from Moscow, Livingston county. In the smaller figure, the concentric
laminae are numerous and sharp, as is the fact in many species of this genus.
2. Delthyris congesta.-View of the upper valve, showing the broad mesial fold, and broad
plain ribs. -
2 a. Front view, showing the elevation of the lower valve into a linguiform extension, and
the deep mesial sinus.
This is a remarkably rotund fossil when pressed, but when compressed, often much re-
sembles the last, and is frequently mistaken for it. The mesial fold, however, is plain, and
the surface free from granulations; the ribs are likewise fewer in number.
3. Delthyris macronota. — View of hinge, showing the broad area and narrow aperture.
3 a. View of the area of the lower valve. - -
3 b. Lower valve.
This fossil is always readily distinguished by the broad area, the narrow aperture, and the
numerous small plain ribs and strong concentric laminae of growth. It is more abundant at
Moscow than in any other part of the district; though it is of frequent occurrence on the
shores of Seneca lake, and in other places.
HAMILTON GROUP.
207
85.
_\º
§§%
§
y
&
º
§
y
º
§
s
s
§
§
ſº
º
º
º
%.
º
Fº º º § º [] sº :§
\
º
º sº -
| -
* º *
º
º § º -
|
ſº
§
º
§
D Ç ºft
sº W §§
sº
%
;
§ i.
208 GEOLOGY OF THE FOURTH DISTRICT,
86.
|
\º\
%%2
8. Delthyris medialis. – View of upper valve and hinge area, with the deltoid aperture.
8 a. Lower valve of the same, showing the broad expanding mesial sinus.
8 b. View of the interior of the lower valve. -
9, and 9 a. Two views of a young shell of the same species??
Upper valve semicircular, much elevated in the middle; lower valve very convex, beak
prominent; surface marked by 32 to 40 rounded ribs, which are crossed by numerous laminæ
of growth. These lines of growth are slightly arched upon the rib, and there is frequently a
depressed line extending along the centre of each, half way from base to beak. The area is
large, curved, and striated transversely.
I find this shell in the State Collection, labelled by Mr. Conrad, D. audacula; but it does
not correspond with the fossil described by him under that name (Jour. Acad. Nat. Sci. Vol.
8, p. 262). This fossil is the most abundant of the Delthyrides after D. mucronata.
Localities—Moscow; Seneca lake; Pavilion; Lake Erie.
10. Delthyris fimbriata (ConRAD, Jour. Acad. Nat. Sci. Vol. 8, p. 263). — Lower valve,
10 a. Cast of the upper valve of the same.
10 b. A small portion of the shell magnified. -
Upper valve sub-elliptical; lower valve nearly circular; surface marked by about twelve
rounded ribs, which are crossed by concentric fimbriated lamellae; beak very prominent.
The shell of this fossil appears very fragile, and the cast is more commonly met with.
Localities—Seneca lake ; Moscow ; York.
HAMILTON GROUP. - 209
Among the numerous corals, the following have been selected as presenting some of the
more common forms.
Q . - 87.
º
bº Wilſº
ſº
t
–23
º
j.
º ſ
º
ift
º Fº |
º |†
§ º: sº
ſº º % i ſ º º f
{\º § |||}
Yº ſ | º
§
º
º §§§
ºğ
ºù) Nº. * s º
§§ §. º ſº § l §
3. §º § -
Ş., º º º
§§
º
§§
º
º
º: l
º
\\
º
W | § % gºtº.
º:
2% 㺠§ 㺠§§
& ºf sº
§ º Nº. iº $º
º
\
º
º º | *** * * º }}".
§§ ||||||}}}
§ sº º
wº º *
t
wººl
º
1. Cystiphyllum cylindricum. 3. Strombodes helianthoides? 5. Strombodes 7 rectus.
2. sº gºss 4. Strombodes distortus. 6. Strombodes simplex.
1 and 2. Cystiphyllum cylindricum. (LONSDALE in Silurian Researches, p. 691, pl. 16 bis,
f. 3, 3 a and 3 b.)— Cylindrical; straight or curved; externally very rugose and striated;
internally wholly vesicular. -
Fig. 1 with Aulopora tuba formis attached; the same is figured with this coral attached, in
Silurian Researches, from the Wenlock limestone. - -
Fig. 2, a smaller specimen, with the bases of crinoidal columns attached. Of these, the one
at a evidently fixed itself while the coral was standing in an upright position; the one at b,
and an intermediate one, evidently began their growth after the coral was thrown down, as
their direction is at right angles to its axis.
Localities—Moscow; York; Eighteen-mile Creek.
3. Strombodes helianthoides? (PHIL. Palaozoic Fossils, p. 11, pl. 5, f. 13. - Cyathophyl-
Ium helianthoidum, Goldfuss, pl. 20, f. 2). —Turbinate, straight or slightly curved near
[GEol. 4th DIST..] 27
210 GEOLOGY OF THE FOURTH DISTRICT.
the base; surface striated and distantly wrinkled; disk expanded, and sub-reflexed at the
margin; cup deep in the centre; lamellae denticulated. The vertical lamellae proceed from
the centre, and there are no transverse laminae as in Cyathophyllum.
Localities—Moscow; York; Seneca lake. -
&
4. Strombodes distortus, n. s.?– Irregularly cylindrical, contracted and expanded by strong
concentric ruge; more or less abruptly curved. The laminæ are spirally contorted in speci-
mens which have been examined.
Localities—York; Moscow; Eighteen-mile creek.
5. Strombodes? rectus, n. s. – General form turbinate, elongated, gradually expanding
from the base; straight; surface marked by longitudinal lines, which indicate the internal
laminae. - -
This is an abundant fossil, sometimes appearing in pairs, but never joined together. It
usually tapers gradually to a very small point at the base. The cup is very deep, and the
margins thin, being usually flattened.
Localities—Moscow; Seneca lake; York; Eighteen-mile creek.
6. Strombodes simplew, n. S.–Turbinate, curved near the base; disk expanded; thin on
the edge, sometimes sub-reflexed; laminae simple, much contorted in the centre, and irregu-
larly bifurcating toward the margin, (about 40 in number;) surface marked by longitudinal
striae. -
The simple prominent laminae, and shallow cup, at once distinguish this species. It re-
sembles the S. plicatum, which occurs in the Corniferous limestone.
Locality—Moscow.
Several other species of these genera occur in the Hamilton group, some of which have
been figured, as well as many other fossils which will hereafter be published, either at the
end of the volume or in the report on palaeontology.
HAMILTON GROUP. - 211
Localities of Superposition in the Hamilton Group.
[See Section along Cayuga lake, Pl. VII.; and Coast Section of Lake Erie, Pl. W.]
The section along Cayuga lake presents this group, succeeded by the Tully limestone,
which is followed by the Genesee slate. The section on Lake Erie presents these two slates
in contact, with merely the intervention of a calcareous band of two or three inches thick.
These points are the two extremes of the district, and between them the Tully limestone has
thinned out, or is only represented by a thin calcareous layer. Notwithstanding this, how-
ever, we find, in all localities examined, that the Moscow and Genesee shales are entirely
distinct, never mingling in any degree.
The following section on the bank of Cayuga lake, at Kidder's ferry, presents the succession
of these rocks. -
1. Olive shale, with Pterinea, Cypricardia, Strophomena, &c. 80 feet.
2. Coarse-grained shale, with large numbers of Fucoides---- 40 feet.
3. A harder calcareous stratum, producing a cascade. - -
4, 5 and 6. Bluish and greyish blue, very fissile shales, with
large numbers of Atrypa, Orthis, Delthyris & Strophomema, 90 feet.
7. Tully limestone ----------------------------------- 11 ft. 8 in.
8, 10 and 11. Genesee slate, embracing a heavy course of sep-
taria, 9; the portion at 11 is highly fossiliferous. Whole
thickness ------------------------------------------- 150 ft.
12, Slaty sandstone, irregularly laminated.
The following is a section of the conical hill on the Crooked lake outlet, being the same
shown in the sketch at the head of the group.
89.
* 4. Genesee slate ----------------------------------------- 7 feet.
== 3. Tully limestone --------------------------------------- 13 “
2. A thin band of black slate. -
I = 1. Bluish, fissile, and compact shale of the Hamilton group -- 60 “
27.
212 GEOLOGY OF THE FOURTH DISTRICT,
90.
25, TULLY LIMESTONE.
This rock marks in a most prominent manner the termination of the fossiliferous shales of
the Hamilton group, and is succeeded by shales of a widely different character. It first ap-
pears within the district on the western shore of Cayuga lake, extending for many miles, and
is readily traced across the county of Seneca to the Seneca lake, where it is exposed upon
both shores, and in the outlet of Crooked lake.
It receives its name from the village of Tully, in Onondaga county, where it is better de-
veloped than elsewhere, and better marked by its peculiar fossils. From this point westerly
it becomes gradually thinner, until it is scarcely recognized. -
The rock is usually thick-bedded, but often divides by numerous irregular seams into small
fragments. Sometimes, however, it is in courses of six inches or a foot thick, and quite close-
grained and compact. In other situations I have noticed it, where the surface was completely
checkered by seams; and on breaking the mass, the whole crumbles into small angular frag-
ments, much in the same manner as the shales containing pyrites. The rock is often an in-
timate mixture of shaly and calcareous matter, the latter greatly predominating. Again it is
almost purely calcareous, with shale in thin seams, separating the rock into wedge-form and
irregular laminae. Its color, on first exposure, is blue, or often nearly black, but weathers
to an ashen hue. From resisting the weather more firmly than the shales, it usually stands
out in the face of the cliffs as a prominent band. It sometimes exhibits a tendency to a con-
Cretionary structure, but this is not usual. .
On the shores of Cayuga and Seneca lakes, its relations to the overlying and underlying
rocks are distinctly seen along a distance of many miles. From where it first appears on the
north, it soon dips to the level of the lake, and again rises to the southward, presenting several
undulations, which continue the mass above the water much longer than otherwise. These
undulations are recognized in the section, Plate VII; and they are even more distinctly marked
on the western side of the lake, and upon Seneca lake.
TULLY LIMESTONE. e 213
The illustration at the head of the preceding page is from a sketch on the shore of Seneca
lake, south of Hathaway's landing, where the Tully limestone is seen to dip from the north,
and pass beneath the level of the lake; and again a few rods farther on, it rises from beneath
the water and ascends southward, disappearing from the shore. About six miles farther south,
it again comes to the level of the lake, and disappears beneath it for the last time.
These undulations appear upon the west side also, and here it makes another ascent from
the lake after its second disappearance beneath it. This place is a short distance south of
Bigstream point, in Yates county. It is merely the top of the arch which appears above the
water, presenting its whole thickness with a few feet of the shale below, and curving gra-
dually downwards in either direction. (See woodcut 91.) - * -
On the eastern shore of Seneca lake, where this rock rises considerably above the water
level, the action of the waves has undermined the softer shale beneath, and leaves the lime-
stone projecting. This process has evidently gone on for a long period, as the shore is skirted
by an irregular wall of the fallen fragments. Thousands of tons of these fragments have been
removed for burning to lime, and those now remaining are mostly beneath water. The practice
of removing these fragments, or of allowing them to be taken away, is of doubtful economy;
for while they remain, they form a barrier which protects the shore from farther encroachments
by the water; but their removal admits a renewed action of the water upon the cliffs, which
undermines the limestone, bringing it down with all the mass above it.
Along the western shores of the lakes this feature is not perceptible, from the short duration
of easterly winds, which have little influence upon the shales. The high perpendicular cliffs
are consequently less common on this side, and the limestone less exposed.
This limestone appears in the banks of the outlet of Crooked lake, being visible almost
continuously from Seneca lake as far as the fall at Wait's mill on the outlet, where it dis-
appears beneath the superincumbent black slate.
After leaving this place and the western shore of Seneca lake, this limestone appears but at
few points farther west. In the bed of Flint creek, at the village of Bethel, it is visible, and
at another point about four miles northwest of this place, in the bed of a small stream. At
the latter point, it is but three feet thick.
A few miles farther west, on Canandaigua lake, it is represented by a few inches of im-
pure calcareous matter, but the character of the shales above and below contrast as strongly
as where the limestone has its greatest thickness. In all localities west of this point, where
the junction of the shales can be examined, we find a few inches of hard impure limestone,
which would scarcely be noticed but for the contrast in the shales, which bear the same cha-
racters as farther east. . -
So far, therefore, as it can be described, this rock is virtually absent at all places west of
Canandaigua lake; still its place is equally marked, and affords a point of reference in all
localities. Its origin was evidently at the east, and from the small quantity of the product, it
has spread over only a small portion of the State. Were it not for the great contrast in the
shale above, and the extinction of the greater part of the organic remains at this point, it might
be united with the last group, being in fact less persistent than the Encrinal limestone which
214 GEology of THE FOURTH DISTRICT.
separates the Moscow shale from that below it. Several of the fossils of this rock are pecu-
liar to it, being unknown elsewhere. The same is true also of the fossils of the Encrinal
limestone, before spoken of in the Hamilton group.
Concretionary Structure of the Tully Limestone.
Near Big-stream point, on Seneca lake, where this limestone rises above the level of the
water, the lower strata exhibit a concretionary structure, and some portions are actually sepa-
rated into regular spherical concretions. The sketch below is a section at this place.
This structure seems to be owing to a meagre supply of the material, which when spread
over the bottom was insufficient to form a continuous stratum, and collected into these spheri-
cal and concretionary masses. Similar effects seem to have occurred in other cases, parti-
cularly in some of the shales where a small portion of calcareous matter has aggregated itself
into spherical forms, presenting a continous course of these, which hold the same position in
the strata as if a thin layer, once continuous, had been rolled up into spheroids.
Localities.—A few localities will suffice for acquiring a knowledge of this rock in the Fourth
District. The western shore of Cayuga lake south of Ovid, and the eastern shore of Seneca
lake, from Hathaway's landing southwards, will give good opportunities of examination. The
western shore of Seneca lake and the outlet of Crooked lake are also equally good localities.
At the village of Bellona, in Ontario county, it is well exposed in the bed of a small stream,
and contains more of its fossils than at any other locality. There are some other points of
minor interest, but they afford the observer nothing new, or of different interest from those
enumerated. * - -
Thickness. –The greatest thickness of this rock within the district is but sixteen feet, and
in most of the localities it is less than ten feet thick. It gradually diminishes westward, and
from Canandaigua lake westward its place is occupied by a calcareous band of three or four
inches thick. - -
Mineral contents.-The rock contains no mineral of interest. The cavities of fossils are
often lined with calcareous spar, and in a few cases some small crystals of sulphate of baryta
have been obtained in similar situations. *
TULLY LIMESTONE. - 215
The mass is too thin to be of importance in its effects upon springs or upon the character
of the soil. It is the most southern limestone in the State from which lime is burned, and in
this respect is important to the inhabitants of the district along which it extends. Being from
six to eight or ten miles south of any other point where limestone is quarried, it becomes of
great value, both for burning to lime and as a rough building stone.
Organic Remains of the Tully Limestone.
As a general fact, organic remains are rare in this rock within the district. In the Third
District, however, they are more common, but they are of the same forms in both. Besides
those figured below, there is a species of Cyathophyllum, which is abundant at Bellona in
some thin shaly layers in the upper part of the rock. In many localities fragments of fossils
are found, though perfect ones are not met with. This seems more extremely so towards its
western termination. - -
92.
2. Orthis resupinata. 3. Atrypa lentiformis. 4. Atrypa affinis.
1. Atrypa cuboides? (Reference, SoweRBY, Geol. Trans. 2d series, Vol. 5, pl. 56, f. 24.
PHILLIPs, Palaozoic Fossils, page 84, pl. 34, f. 150.)—Sub-globose or cuboidal; front mar-
gin of the lower valve extremely elevated, occupying a deep sinus, with nearly parallel sides
in the upper valve; lower valve, with the exception of this process, nearly flat; beak small.
This fossil is readily known by the square sinus of the upper valve, the strongly ribbed
process which fills it, and the sharp edges of the shell at the junction of the valves. It seems
scarcely possible that this shell can be different from the English specimens, though both
Sowerby and Phillips describe the A. cuboides as having fifteen ribs on the mesial sinus,
while ours has but from six to eight. In other respects there is a precise correspondence.
The ribs on the process of the lower valve, and on the elevated portion of the upper valve,
are much stronger than elsewhere on the shell. •
Locality—Bellona, Ontario county.
216 GEOLOGY OF THE FOURTH DISTRICT.
2. Orthis resupinata (PHILLIPs, Palaeozoic Fossils, p. 67, pl. 27, f. 115. Spirifera resu-
pinata of same author, Geol. of Yorkshire. Terebratula resupinata, Sow, Min. Conch. tab.
325. Anomites resupinatus, MARTIN. Orthis Tulliensis, Report of Third District, page
163.)—Transversely elliptical; lower valve very convex, slightly flattened in the centre;
upper valve convex near the beak, and depressed in front; surface finely radiated.
When the shell is partially or entirely removed, the surface appears covered with minute
punctulations. From comparison of specimens, Mr. Conrad says this fossil is identical with
those sent from England under the name of Anomites resupinatus. It occurs in the mountain
limestone of England, and in rocks of the same age as the higher shales and sandstones of the
New-York system.
3. Atrypa lentiformis (WANUXEM, Geol. Report, page 163). —I am not able to discover
that this fossil differs from the Atrypa affinis in some of its various appearances. It is usually
smaller in this rock than that fossil generally is; but in the next figure is another form, appa
rently of the same fossil, from this rock.
4. Atrypa affinis. (For synonymes and authorities, see page 198.)—The valves of the
shell are much compressed at the margins, giving it the appearance of being surrounded with
a fringe. The specimens, as commonly obtained, are only that part of the figure which ap-
pears more prominent.
I am indebted to Dr. H. P. Sartwell, of Penn-Yan, for the specimen from which this figure
is taken; and also for specimens of the Atrypa cuboides?
Locality—Bellona, Ontario county.
The figure in the margin is a front view of Atrypa cuboides? the
others not being quite satisfactory in regard to the form and appearance
of the ribs on the mesial sinus The elevated portion of the lower
valve is not quite as great as in Mr. Phillips's figure. I have not the
means of referring to Mr. Sowerby's figure at this time, but that is the
one by which I had identified this fossil as I then supposed.
For localities of superposition of the Tully limestone, see that head under the Hamilton
group.
ºßMARKS, 217
REMARKS, PRELIMINARY TO THE FOLLOWING ROCKS AND GROUPS.
In the Fourth District, the Tully limestone terminates all those deposits in which calcareous
matter forms an essential part. In all the higher rocks, this material, when existing, is the
result of the destruction of organic bodies; and in the few instances where it appears, the
origin is unquestionable, for the fossils still retain so much of their original form as to be rea-
dily recognized. This rock forms a strong line of demarcation not only in this respect, but
also as regards fossils, very few forms which are known below continuing into the rocks above.
The lithological character of the products above this rock are throughout more or less similar,
while they differ from those below ; and with a single exception, lithological character is a
sufficient guide for distinguishing the different strata.
This contrast of character is more marked towards the western extremity of the district,
than it is farther east; and finally, on its eastern extreme, there is a greater similarity in the
lithological features. This change is likewise attended with the occurrence of some of the
fossils of the lower group in the rocks of the higher, the nature of the two being very similar,
although the Tully limestone is in its greatest force; while at the west, where it does not
exist, no such mingling of the fossils is known. .
At Ithaca, for example, where we are far above the Tully limestone, and where the rocks
are well marked by an abundance of fossils peculiar to themselves, still we find the Microdon
bellastriata, the Modiola concentrica and some others, and I have even detected the Calymene
bufo and Dipleura Dekayi in the same association. Still farther east, there is a greater min.
gling of species of the lower rocks with the upper, and a nearer approach constantly in materials
of composition. These circumstances, in the eastern portion of the State, render it difficult
to point out the line of demarcation between the lower and higher rocks of this division.
At the eastern extremity of the State, also, the Tully limestone does not exist, and therefore
that guide to the line of division between the lower and higher groups is wanting. The ab-
sence of this rock, and the similarity of lithological products as well as the mingling of the
organic remains of the lower rocks, renders it impossible to make a distinction in groups with
the same degree of satisfaction as farther west. By reference to the section along the Genesee
river (Plate 13), it will be seen that the Genesee slate, a black carbonaceous mass, is suc-
ceeded by shale of a deep green color, and well defined above. This is succeeded by flag-
stones, which alternate with shale of a less deep green color, and often with black shale.
These again are followed by a greater proportion of sandstone, often thick-bedded, and pre-
senting far less of the characters of those below. -
These rocks are well exposed on the Genesee river, and there can be no possible room for
error in their examination. The whole thickness here exposed is scarcely less than one thou-
sand feet; and throughout this thickness, there is as yet no fossil known which occurs in the
Chemung group to the south and above these rocks. These circumstances led to the separa-
tion of this portion of the system, and the adoption of Portage or Nunda as the locality de-
[GEOL. 4th DIST.] 28
218 GEOLOGY OF THE FOURTH DISTRICT.
signating the group. Farther east the green shale (Cashaqua shale) is often darker in color,
and more sandy, becoming largely interstratified with flagstones which have much the character
of those which lie above it on the Genesee, except in the absence of a peculiar species of
Fucoides. At the same time, the small Avicula, which is so abundant in the Genesee slate,
is almost equally abundant in the green shale and flagstones at Penn-Yan.
Again, when we go westward as far as Lake Erie, we find, that instead of the flagstones
succeeding the green shale as on the Genesee, a black shale is the first mass above. This
soon gives place to green shale; and we have alternations of green and black shale for many
hundred feet, before coming to the thin-bedded sandstones.
26. GENESEE SLATE.
Upper Black slate, and Black shale and slate, of the Annual Reports.
(PART of No. 8? PENNsylvania SURVEY.)
[Lower part of P. woodcut, page 27. See also Sections, Plates W. and VII., and County Sections.]
Superimposed upon the Tully limestone, or, in its absence, resting upon the Moscow shale,
we find a great development of argillaceous, fissile, black slate. Where its edges only are
exposed, it withstands the weather for a great length of time, and often presents mural banks
in the ravines, river courses, and upon the shores of lakes. Where the surface of the strata
are exposed, it rapidly exfoliates in thin even laminae. On disintegration, it is often stained
with iron, owing to decomposition of pyrites; but in many instances, and the greater number
of localities, it retains its deep black color. In this it is distinguished from some beds of
black slate in higher situations, which always become stained with hydrate of iron on their
edges, and upon the surface of the laminæ. -
In color and general characters it greatly resembles the Marcellus shale; and aside from
position, it would be difficult to distinguish the two in the absence of fossils.
Constituting a part of the great series of shales, with flagstones and thin-bedded sandstones,
which occupy all the southern range of counties, it forms no conspicuous feature in the scenery
or topography upon the general surface. In ravines and river banks, it is usually seen in
connection with the rocks below or above, or with both, and forms only an element in the deep
escarpments. Its greatest development in the district, and a point where it appears more
prominently alone, is at the opening of the gorge of the Genesee river at Mount Morris."
–º
* From the circumstance that other shales above this appear in the same gorge, it would have been desirable to give an-
other name; but no locality is known, which is not more objectionable than this. Since it is very probable, also, that this
(GENESEE SLATE, 219
The mass decomposes much less rapidly than the soft calcareous shales below it, and the
thin slaty laminae resist atmospheric action for a long time. On the Genesee it presents two
regular courses of concretions or septaria, with numerous single ones scattered through it
without order. These are often divided by seams of crystalline matter; but many of them
are without these seams, the inside being entirely composed of crystalline carbonate of lime
of a deep resinous color, from its strong impregnation with bitumen, which often flows from
the small cavities when the mass is broken. . • , ,
In lithological character this rock is entirely uniform throughout the district, presenting
itself upon the margin of Cayuga lake and upon Lake Erie, having the same deep black color
and laminated slaty structure. Neither is there any change in its organic remains; the same
forms, and many of them almost equally abundant, are found throughout its entire extent.
The greater portion of this rock is destitute of fossil remains, and it is only toward the upper
part that they occur. - -->
The position of this formation on the map is at the junction of the purple and brown colors;
it being too thin a mass, and occupying too little surface, to be represented by itself. In the
Fourth District this rock borders the margins of Cayuga and Seneca lakes, and is visible in
all the deep ravines, forming high cliffs above the Tully limestone, which latter always pro-
jects boldly, forming a cliff, or a cascade on all the small streams. It crosses Seneca county
in a curve, its extreme northern limit being some distance north of the village of Ovid, while
its final disappearance to the south on the lake shore is ten or twelve miles distant. This
circumstance is owing to the great height of the central part of the county above the lake, the
highest part of which is between 400 and 500 feet above the level of the water of Seneca, and
more than 500 above Cayuga lake. On the western side of Seneca county, this rock extends
as far south as the town of Starkey in Yates county; and from thence it sweeps around in a
northwest direction through the towns of Benton, Seneca and Gorham, and stretches south-
ward along Canandaigua lake, to within a few miles of its southern extremity. From this
place westward its outline is extremely irregular; and in the western part of Ontario county,
it forms some small outliers in the towns of Bristol and Richmond. From the outlet of Co-
nesus lake in Livingston county, its direction is southwesterly, till it comes to the level of the
Genesee valley in Groveland and Mount-Morris. From the western side of this valley, its
course is northwesterly to the south part of the town of York, whence it continues westward
to Allen's creek. Beyond this point it extends northwesterly into Bethany, and thence by an
irregular west and southwest direction to Lake Erie.
The outline and direction of this rock is interesting, as showing the southern limit and
extent of the Hamilton group. The irregularities in outline, and the great southern depres-
rock will in future be considered only as a member of the Portage group, its local name will be the more appropriate. The
aboriginal name of this place was Squakie Hoh; and the gorge at its outlet received the name of Squakie Hondah, which
signifies a gorge with a river opening into a plain, which is beautifully applicable to this spot, where the river, after pursuing
a meandering course for twenty miles through a deep gorge, and over three successive cascades descending more than five
hundred feet, flows out into the beautiful broad and fertile valley of the Genesee. These aboriginal names have been fur-
nished me by E. N. HoRSFORD, Esq.
28*
22%) GEOILOGY OF THE FOURTH DESTRICT,
sions, are owing to deep valleys, as those of the lakes and the Genesee river. As it approaches.
Lake Erie, it takes a broad sweep to the southwest, and disappears beneath the surface of the
lake in the town of Evans in Chautauque county.”
The uniformity in lithological character of this mass throughout, and its finely levigated par-
ticles, indicate a quiescent period, and the operation of an ocean moved only by gentle cur-
rents. There is no great accumulation in one part over another, and the deposition appears
only to have been affected by the common law of gravitation. At the time of its deposition it
possessed the character of a soft, black, carbonaceous mud, with scarcely an admixture of
siliceous matter in any part. -
Concretions.—The well defined concretions or septaria have been noticed, and these are
all that occur throughout the mass to interrupt its sameness. These bodies are often without
any apparent seams; at other times they are crossed in various directions by seams of crys-
talline carbonate of lime, etc., which apparently fill cracks previously formed by the desicca-
tion of the mass. These concretions are interesting as showing the occurrence of calcareous
matter at one or two positions in the rock, which, though small in quantity, spread over a large
extent of surface. * -
These bodies vary from the diameter of a few inches to two or three feet, and are usually
pretty purely calcareous and nearly spherical.
Localities.—A few points will suffice to give the observer a knowledge of this rock. In
Seneca county it can be examined in nearly all the gorges which communicate with the lake,
in the towns of Ovid, Lodi and Covert. Below the Lodi falls it abounds in fossils peculiar
to it, though of few species, Orbicula and Lingula being the most abundant. About two
miles south of Big-stream point, in Yates county, it is well exposed on the lake shore, and
contains its usual fossils. Along the outlet of Crooked lake it is well developed, and also in
the ravines on the south side of this place. There are several good points for examination
on the banks of Canandaigua lake, and in the ravines leading to the same.
The gorge of the Genesee river at Mount-Morris affords, probably, the best exposition of
this rock, where it is laid open in the perpendicular cliffs on either side, for more than a mile
in length. The principal fossil at this place is a species of Avicula with a very fragile shell,
which will be seen figured in illustration No. 94. The shale is well exposed in a ravine,
and at a fall on a small stream about two miles northwest of the village of Moscow, in Living-
ston county. -
From this place to Lake Erie it may be examined in nearly every ravine which extends
southward, and in the lateral ones joining the north and south valleys. Its constant fossil is
the little Avicula just referred to, and in nearly every locality it abounds, frequently covering
the surface of the slaty laminae, through several inches in thickness, and more sparingly
scattered through a greater extent.
* It will be recollected that the surface of Lake Erie is about 120 feet higher than Seneca lake, and consequently this rock
disappears beneath its surface four or five miles farther north than if it were at the same level.
GENESEE SLATE, 22}
On the shore of Lake Erie it may be examined in numerous places, but the best locality
is at Eighteen-mile creek and along the banks of the creek a mile from the lake. It is here,
if possible, more strongly marked by the Aviculae, and they are so crowded together that
often, for many feet in extent, it is nearly impossible to distinguish their forms.
Thickness.-On the shores of Seneca lake and in Ontario county the thickness of this rock
is about 150 feet, as estimated by careful measurements along the descent of streams and in
perpendicular banks, though there is no single point where the whole thickness is shown at
once. After passing the Genesee river in a westerly direction, it soon becomes evident that
the rock has diminished in thickness, though there are no points where good measurements
can be obtained. On the shore of Lake Erie, however, the whole rock is well exposed, in
connection with the lower and higher masses, in the perpendicular cliff at the mouth of Eigh-
teen-mile creek (See section, Plate 5.) At this place its thickness is but twenty-three feet.
seven inches, or less than one-sixth of its thickness at the eastern limit of the district. This
thinning is due to the cause before mentioned, viz. the diminishing power of the currents.
which transported the materials, and the consequent precipitation of a greater portion of the
matter near the origin of the same. It bears no evidence of denudation, and, from the even
surface of the rock below, this great diminution is not local, but has evidently been gradual;
and uniform through the extent of one hundred and fifty miles.
Minerals of the Genesee Slate.
The only minerals, except iron pyrites, which occur in this rock are found in the cavities.
of the concretions. These are crystallized carbonate of lime, in the common rhombic forms,
and in hexahedral prisms with trihedral summits; sulphate of baryta; quartz crystals, with
more rarely galena, or sulphuret of lead. Fluid bitumen is of common occurrence, and with
it a bright blue fluid and a substance like spermaceti, but softer. These are volatile, and it
has been impossible to preserve any of them. The fluid bitumen and the blue fluid have
likewise been noticed in septaria in the Marcellus slate. r
This shale is so intimately blended with the rocks that follow, that alone it has exercised
no influence on the soil or springs which is not common to the rocks above it, and are only
such as will be subsequently noticed under the next group.
Organic Remains of the Genesee Slate:
The only constant fossil of this rock is the Avicula fragilis, figured below. The greater
part of the mass is destitute of any organic remains, and it is only in the higher portion that
we find them in very considerable numbers. The forms figured in the woodcut (No. 95) are
usually found in the upper strata, and I do not recollect having ever seen any of them more
than twelve or fifteen feet below its termination. In several localties on Cayuga and Seneca
lakes, these forms are all found associated together, and in great numbers; but farther west
222 GEOLOGY OF THE FOURTH DISTRICT.
they are more rarely found, and finally do not appear at all. The Avicula, on the other hand,
appear to increase in numbers in a westerly direction, and on Lake Erie are more numerous
than at any other point. . -
With the termination of the Moscow shale, seem to have perished the immense number of
organic forms which every where mark the presence of that rock. For a long period, as is
evident from the character of this shale, the ocean bed was not inhabited by living things; and
with the exception of the few species in the Tully limestone, where that rock occurs, it is not
until we arrive at nearly the termination of this slate, that vitality again assumes its place
among the laws of nature, to go on increasing, till in the upper part of the Chemung group
the ocean literally swarmed with living things.
I and 2. Avicula fragilis. 3. Strophomena setigera. 4. Tentaculites fissurelia.
1 and 2. Avicula fragilis, n. S. – Shell ovate, (hinge line being usually concealed,) very
thin; surface marked by concentric lines, and a few faint radiating striae; hinge line shorter
than the width of the shell.
Fig. 1 is a small fragment of the shale, with these shells covering the surface.
Fig. 2, a single shell, showing the perfect form.
It is an extremely abundant fossil, but from being mutilated, and often partially concealed,
its generic relations are not always readily detected. It occurs in the Marcellus shale.
Localities—Seneca county; Geneseo; Leicester; Mount-Morris; Eighteen-mile creek.
3. Strophomena setigera (see page 180 of this Report). This fossil is also common to the
Marcellus shale. -
Locality—Outlet of Crooked lake.
4. Tentaculites fissurella. A fragment of the shale covered with the fossil (see page 180 of
this Report). Occurs likewise in the Marcellus shale.
The three species here figured are all common to this rock and the Marcellus shale, the
lithological character of the two being precisely similar. Neither of them have been noticed
in the intervening rocks of the Hamilton group, though the Avicula passes upwards into the
Cashaqua shale of the Portage group. This is an interesting example of the recurrence of the
same species of fossils in rocks widely separated from each other. This identity in fossils,
and similarity in lithological characters, has been the cause of frequent mistakes in identifying
the two.
GENESEE SLATE, 223
The following species, figured in the Report of the Third District, page 168, are quite
abundant in this rock in the eastern part of the district, but are far less common farther west,
and disappear altogether before reaching Lake Erie. -
95,
}, Orbicula Lodensis, 2. Atrypa (Orthis) quadricostata. 3. Lingula spatulata. 4. Lingula concentrica.
1. Orbicula Lodensis.-The shell is concentrically striated, and marked by a few radiating
lines. It differs from one in the Hamilton group, in being much smoother.
Localities—Lodi in Seneca county, below the Falls; Big-stream point.
2. Atrypa quadricostata. — Mesial portion of the shell marked by four or five strong ra-
diating ribs; sides nearly plain.
Occurs with the last.
3. Lingula spatulata. —This is an abundant little fossil in the localities named above, and
is readily distinguished by its small size and spatulate form.
4. Lingula concentrica. —This fossil is peculiar for its great proportional breadth at the
beak, and the extent of the margin beyond. Some specimens seem scarcely referable to the
genus. - -
Occurs with the preceding species at Lodi, and near Bigstream point.
For localities of superposition of this rock, see that head under Hamilton group.
224 GEOLOGY OF THE FOURTH DISTRICr.
ſº
ºº:
ºfºº }º &
ºjºſ. º §§||
ºiſſºl
º ...)
º
|
º º
º
l Jºº.
§:
|
#º
--
;:
Opper and Middle Falls of Portage. From a sketch by Mrs. HALL.
27. PORTAGE OR NUNDA GROUP.
Sherburne flagstones and shale, Cashaqua shale, Gardeau and Portage groups, of the
Annual Reports.
(PART of No. 9, PENNsylvania SURVEY.)
{See P of woodcut, page 27, and section of Genesee river, Pl. XIII; also section of Lake Erie shore, Pi. VII.]
This group presents an extensive development of shale, shales and flagstones, and finally
some thick-bedded sandstone towards its upper part. Like all the other mechanical deposits
of the system, as they appear in New-York, it is extremely variable in character at different
and distant points. From its general similarity, and from the difficulty also of separating it
from the higher rocks on its southern limits, it is colored the same tint on the map, being the
northern part of the light umber tint. - -
From its superior development along the banks of the Genesee river in the district formerly
included in the town of Nunda, now Portage, it has received that name to distinguish it from
the higher rocks, which possess some differences in lithological characters, but a more striking
dissimilarity in organic remains. -
PORTAGE GROUP. 225
This group rises sometimes in a gentle slope, and at other times abruptly from the softer
shales below. The enduring sandstones of the upper part have enabled it to withstand de-
nuding action to a considerable degree, and these often extend far northward on the elevated
grounds between the deep north and south valleys, presenting a gentle northern slope to the
shales of the Hamilton group; while on the sides of the same hills the slope is abrupt, and
the surface being but little covered with northern drift, the valleys are bounded on either side
by steep hills. This character is well illustrated along the southern part of the Genesee valley
towards Dansville, and in the valleys of Allen's creek, the Tonawanda, and the different
branches of the Seneca and Cayuga creeks. The same is also seen in the valleys of Mud
creek, Flint creek, Canandaigua lake, and to a greater or less degree along all the valleys and
streams which extend into this group. - -
The change in the external appearance of the country indicates the commencement of these
rocks, although they are not seen. The valleys just spoken of, in their course through the
shales of the Hamilton group, present gently sloping sides, and the country rarely rises far
above the level of the valley bottom or bed of the stream. On approaching the northern margin
of the Portage group, the observer finds a gradually increasing elevation of the hills on either
side, and an abruptness in their slope; and in a short time he finds himself in a deep valley,
bounded on either side by hills rising four or five hundred feet, and in some instances even
eight hundred feet above the bed of the stream. These elevations often extend several miles
unbroken, except partially by the deep ravines which indent their sides, and which have ori-
ginated in recent or ancient water courses which took their rise upon the summits of these hills.
The higher sandstones of the group, and in many instances some of the intermediate ones,
produce falls in the streams which pass over them, and some of the most beautiful cascades
in the State are found among the rocks of this group. The highest perpendicular fall of water
in the State is produced by the rocks of this group, and in none others do we meet with more
grand and striking scenery. The pedestrian often finds his course impeded by a gorge of
several hundred feet in depth; and in the very bottom of this, and scarcely perceptible, is the
winding stream, the only representative of the once powerful torrent that has excavated the
deep channel. Farther on, above or below, he may see the little stream dashed over a pre-
cipice, and almost disappearing in spray before it reaches the bottom; here, however, it gathers
itself in a deep pool, from which it flows on quietly as before, or gurgling and dashing through
the fragments of the fallen cliffs, it finds its way into the gently sloping valley of the softer shales.
So numerous are these falls in the district, that to present even an enumeration of them
would fill a page. Among these have been selected for illustrations, either from their beauty
and interest, or from being accessible places, the following: Portage Middle and Upper Falls,
Portage Lower Falls, Taghannuck Falls," Hector Falls, and Lodi Falls. The first of these, the
illustration at the head of the preceding page, is the locality giving name to the group. The
river in view is precipitated over two falls of 66 and 110 feet respectively; and below the last,
the rocks rise in perpendicular cliffs of 350 feet in height.
*This is the aboriginal name; the place is usually known as Goodwin Falls.
IGEOL, 4th DIST.] - - 29
226 GEOLOGY OF THE FOURTH DISTRICT.
On the Genesee river, which affords the best development in the district, this group admits
of the several subdivisions shown in woodcut 97 at the foot of the page.” -
:=&º: §§§
ſº
*
§
*%
É
View on Cashaqua creek. From a sketch by Mrs. HALL.
I. CASHAQUA SHALE.
This rock, in lithological and fossil characters, differs sufficiently from those above to be
considered under a separate name. From its perfect development upon the Cashaqua creek,
that name was applied to it before the examinations of the higher rocks had been completed.
1. Genesee slate. 2. Cashaqua shale. 3. Gardeau shale and flagstones. 4. Portage sandstones.
The lowest rock here represented rests on the Genesee slate, and about eight feet from its base is marked with a band of
black shale, similar to the Genesee in every respect. The three divisions of this group, as given in the woodcut, are plainly
recognizable on the Genesee river, and to a great extent over the whole district. As we go east from this point, however,
there is a constant increase of arenaceous matter, and in a westerly direction an increase of mud on shale. The whole ean
be better described under the three divisions above noticed.
PORTAGE GROUP. '. 227
The mass at this place is a soft argillaceous rock of a green color, rapidly crumbling on
exposure, and forming a tenacious clay. From the influence of atmospheric agency, it is very
difficult to procure good specimens; and fossils not being abundant, they might be easily over-
looked. It is, however, marked by certain species of shells which have not been seen in any
other rock, and these have been found to hold the same position over an extent of 150 miles.
On the Cashaqua, and in other places in the same neighborhood, it contains some flattened
concretions of impure limestone, and sometimes of sandstone, but of these it presents no con-
tinuous layers. It is deeply excavated, presenting high and abruptly sloping banks, which
project into the valley on one side and recede on the other, as the stream winds along its
course below. In looking down the stream, as represented in the woodcut at the head of the
page, the slopes of these cliffs are free from vegetation, while on the opposite side they are
entirely covered, often with large trees. This effect is produced by the action of the meander-
ing stream, which flows in its channel from one side of the gorge to the other, continually
undermining the rock which crumbles down from above, thus constantly presenting a fresh
surface. - - |
At the eastern extremity of the district, and on the shores of Seneca lake at Penn-Yan and
other places, this rock consists of a green shale with thin flagstones, and interlaminated sandy
shale. It contains the same fossils; and holding the same position as on the Genesee, it can
be regarded only as the same rock, the intercalation of sandy strata being due to its proxi-
mity to the place of origin. Farther east it is not recognized as a shale at all, the mass con-
sisting of thinly laminated shaly sandstone. At Penn-Yan it often manifests a concretionary
structure, and the Sandy strata are irrregular in thickness and continuance. -
On tracing it west of the Genesee, it constantly presents the same features as on the Casha-
qua creek, though the lower part is occasionally dark colored, and separated from the Gene-
see slate by a thin calcareous band. It is exposed in numerous streams and ravines, the most
important of which are those in the hills bordering on Allen's creek, Tonawanda creek, and the
branches of Seneca and Cayuga creeks. It appears at the village of Wyoming, in Wyoming
county, and in numerous other points in the same neighborhood. On the shore of Lake Erie
its whole thickness is seen in the high perpendicular cliff, having thinned from 110 feet on
the Genesee to 33 feet at Eighteen-mile Creek. At this place it retains all the characters
which are peculiar to it on the Genesee, having changed only in thickness.
2. GARDEAU SHALE AND FLAGSTONEs.
Along the Genesee river, above the last described rock, we find a great development of
green and black slaty and sandy shales, with thin layers of sandstone, which form beautiful
and durable flagstones; these are quarried from the same situation in many places in the
district. The rocks of this part of the group form high, almost perpendicular banks on the
Genesee, only indented by the incipient ravines caused by slides and the action of running
water. From their great exposure along the Gardeau reservation, that name was adopted in
29*
228 GEOLOGY OF THE FOURTH DISTRICT.
the annual reports, to distinguish this part of the formation; and since this is a good point for
investigation, it is described as a subordinate part of the Portage group. -
In the lower part of this subdivision the shales consist of alternations of green slaty and
sandy shale with black slaty shale, one or two thin courses of sandstone occurring in the space
of four or five feet. As we ascend, the arenaceous matter increases in quantity, the layers are
thicker and more numerous, and the shale forms distinct alternations of black and green,
often many times in succession, within the space of fifty feet. Towards the upper part the
courses of sandstone become too thick for flagstones, and the shale is in thicker masses than
below. -
These characters, however, which are sufficiently obvious in the gorge of the Genesee, are
not constant for any great distance in either direction. Toward the east the arenaceous strata
augment in a great degree, to the exclusion of the shales; while in a westerly direction the
sandstones are constantly disappearing, and the proportion of shale constantly increasing. At
the western limit of the State, along the shores of Lake Erie, the Cashaqua shale is succeeded
by a thick mass of black shale, and this is again succeeded by alternations of green and black
shales for several hundred feet upwards, the flagstones having entirely disappeared from
nearly the whole thickness. With the absence of sandy strata and the augmentation of shale,
a few fossils, which were rather sparingly seen along the Genesee and in the eastern part of
the district, become more numerous, and form a distinguishing feature of the rock,
3. PoRTAGE SANDSTONEs.
The thick-bedded sandstones at Portage form the terminal rocks of the group. These are
well exposed in the deep gorge below Portageville, where the perpendicular cliffs rise to the
height of three hundred and fifty feet. The upper part consists of thick-bedded sandstone,
with little shale; while below, the sandy layers become thinner, with more frequent alterna-
nations of shale. The thick-bedded character of the sandstones, and the presence of fucoids
passing vertically through the strata, induced the separation from the rocks below, where the
characteristic species of the same genus lies horizontally upon the surface of the strata. The
lithological character of the sandstone, and the presence of the vertical fucoid, hold uniform
over a considerable extent; and the presence of the latter alone is often sufficient to decide
the position of the rock, where it is but slightly exposed.
Toward Cayuga lake, the increase of arenaceous strata below has rendered a distinction
between the two of little importance; and farther west, where the Gardeau division has be-
come very shaly, the higher division has taken the character which the former one has on the
Genesee, being composed of alternating thin-bedded sandstone or flagstones and shale.
Along the western limit of the State there are but few points where the thick-bedded sand-
stone, like that at Portage, can be seen. One of these is at Laona, and another, which is the
terminating mass of the group, is at Shumla. Along the lake shore it appears at several
places; and in the excavation for the New-York and Erie railroad, west of Fredonia, the same
rocks are exposed.
PORTAGE GROUP. 229
The description of these three divisions will furnish a correct idea of the lithological cha-
racter of the group. At the eastern end of the district the whole series consists of shales and
shaly sandstones, with some thick-bedded sandstones, corresponding more nearly with those
above them than the same do farther west. Still it must be acknowledged that inlithological
characters there is no abrupt change, or evidence of very different conditions in the ocean from
which they were deposited, from the termination of the Tully limestone, to the final deposition
of the Chemung group. Shales and sandstones, differing in some degree, it is true, compose
the whole assemblage. In the lower part these are more intermingled, and the sand is finer;
while in the higher part of this series, the sand is often coarser, and generally less intermixed
with shale. The Portage group forms the lower member of this great division, the sandstones
and shales being less separated than above; the arenaceous strata are finer grained, and
always more argillaceous than in the Chemung group. -
When we apply the test of organic remains, we find an equally, or even more strongly
marked difference in the two groups, and upon this alone a distinction between the two should
be made. Throughout the whole thickness of the Portage group, which is not less than 1000
feet, there are but two forms which can be referred to the Brachiopoda; one of these is a
Delthyris, and the other apparently an Orthis, and both are quite unlike any others which
have been seen in the rocks above or below. In both the Hamilton and Chemung groups,
shells of this family are the predominating forms, and they are at least ten times more nume-
rous than any others. In the Portage group the principal forms are Goniatites (fragments of
several species being known), Bellerophon, and bivalve shells allied to Pterinea? with a small
Avicula everywhere characteristic, and known in no other rock.
Considering these facts, it seems desirable to separate these lower rocks, that we may have
an opportunity of investigating them separately, and of comparing their fossils before we unite
them with the higher group, which has a very great development, and in which I have never
seen one of the fossils of the Portage group. -
The higher mass of sandstone of the Pörtage group, before mentioned, is very persistent,
being known in Ohio as the Waverly sandstone; and there, as well as in New-York, it forms
a line of demarcation between the almost non-fossiliferous shales and sandstones below, and
the highly fossiliferous sandstones and shales above, which latter are a continuation of the
Chemung group. From the circumstance that but few of the strata in the Portage group
contain fossils, they have usually been overlooked, and the rocks on a hasty examination would
be pronounced non-fossiliferous. .
Along the shore of Lake Erie, the rocks of this group hold a conspicuous place, having
traced them continuously from near Eighteen-mile creek in Erie county, to Erie in Pennsyl-
vania; and beyond this they appear at numerous points, apparently being continuous as far
as Cleaveland in Ohio. Fossils, with the exception of fucoids, are rare throughout this whole
distance, and it is mainly from lithological characters that the strata are recognized. In Ohio,
and to the southwest, there is a much greater similarity in the lithological characters of the
Portage and Chemung groups than in New-York, and there they are not separated by those
who have described them. -
230 GEOILOGY OF THE FOURTH DISTRICT,
Diagonal lamination.—This structure, which indicates the mechanical process of deposition,
is of frequent occurrence. In many of the flagstones these lines of deposition are marked by
thin laminae of shale, and again the layer thins entirely out. The process is readily under-
stood to be that where the sand is carried on and spread over the surface, sloping off towards
one side farthest from its origin. The next deposition covers this sloping side necessarily in
the same manner, producing the oblique lines which are often seen in these flagstones.
Ripple marks are abundant in the sandy shale, or where the shale becomes interstratified
with sandstone, but it is often difficult or impossible to obtain good specimens. They are
irregular or unequal generally, but in some instances are well preserved. Many of them have
the appearance of having been produced by a “chopped sea,” or that where a current opposed
the direction of the wind. The same effect is often visible on sandy beaches where the
tide has ebbed; the surface being broken into short, interrupted and irregular ripples, pro-
duced either by the tidal current opposing the wind, or some other similar cause, always
readily understood. That such circumstances operated at the time of this deposition, and
that the sea was alternately shallow and again deeper, is proved at every step among these
strata. The deposits of dark and green argillaceous shales bear no evidence of ripples or
diagonal lamination, and from their homogeneous nature were probably deposited in deep
water, while all the sandy shales and alternations of shale and sandstone bear evidence of
a shallow sea. It is true that the homogeneous mud would not retain ripple marks or
lines of deposition, but from its nature and the attendant circumstances we infer that it was
deposited in deeper water and under a more quiet condition than the sandy strata.
Casts of Shrinkage cracks. – These have been described under the Medina sandstone, and
in the Portage group we again meet with them, though not so prominent or so large as in
the former. - +
These marks are upon the under surface of an argillaceous sandstone which rests directly
upon a soft black shale. The shale became cracked by exposure above water, and the sandy
matter subsequently deposited filled the fissures. -
Concretions, – This group throughout presents a great variety of concretionary forms.
The strata, however, are all uniform, and rarely give any appearance of concretionary struc-
ture in themselves. The concretions are more or less calcareous in the different parts of the
group and in different shales. The more perfectly spherical with seams of crystalline matter
are found in the black shale, while the forms varying from this to the very flat or lenticular
ones are found in the shales varying from blackish to greenish black and green. The black
varieties of shale are always more or less slaty, while the green varieties are not slaty, but
present the marly or indurated mud-like characters, and instead of separating into laminae,
crumble into irregular fragments. - -
The more spherical forms are due to a higher degree of crystallization which results from a
larger proportion of carbonate of lime, while the flattened forms are less crystalline, and con-
sequently less spherical from the larger amount of argillaceous matter.
PORTAGE GROUP. 231
These forms are too well known to require description, but they often assume some fan-
tastic shape which causes them to be mistaken for an organic body. This arises from the
seams on the surface, which are fancied to resemble the lines of suture in the shells of the
tortoise or turtle, and by this name they are frequently known in the neighborhood where
they occur plentifully. From the great number of these in some parts of this group, they
frequently join each other, and assume many of the singular forms which we meet with in
“clay-balls,” or concretions in ordinary clay, which, however, rarely attain more than a few
inches in diameter.
The following form is so unique that it seem
sworthy of illustration, as showing the imita-
tive power of concretionary force. - -
- ===&\ºmmºngº * *
§ºiſſiº £:T
* -----
Cºretion or Septaria, one third the natural size,
232 GEology of THE FOURTH DISTRICT.
The specimen is from the shore of Lake Erie, where hundreds are annually thrown down
upon the beach by the undermining action of the waves. The usual form of these bodies
where this one was obtained, is that of a flattened spheroid. Great numbers of these are
burned for hydraulic cement between Dunkirk and Portland harbor, and they produce a very
good material for this purpose. At the locality alluded to, they are frequently two or three
feet in diameter, and not more than half a foot thick. There are several of these in the State
Collection, showing the varying forms and different sizes. *
In the black shale near Sturgeon point, I saw one of these concretions, almost spherical in
form and six feet in diameter.
On the Genesee river these concretions are often of the size and form of common loaves of
bread, and many of them present the structure of “cone in cone.” This structure occupies
from one to two inches on the outer surface of the concretions. The same structure is also
found in some wedge-form layers in the same situation, both on the Genesee river and on
Lake Erie shore, and it is well known along nearly the whole distance from Chautauque
county, New-York, to Cleveland, Ohio. I have not had an opportunity of ascertaining whether
it holds precisely the same position throughout, but in the western part of the State, its posi-
tion is the same for more than one hundred miles in extent. Many beautiful specimens have
been obtained from Erie, Pennsylvania, and other places in that neighborhood.
100.
\º
º º
º
º
§ | º
Sº
* > . . . . .
Cone in Cone.
The woodcut illustrates the usual appearance of this curious structure. The mass is of a
peculiar kind of clay, and the cones are often composed of concretive laminae, presenting a
transversely striated or wrinkled surface; they are also striated longitudinally.
Fig. 1, represents the common structure of the mass. Fig. 2, is a single come detached
from the others. - -
Casts of flowing mud.
The phenomena presented in these bear some analogy to a concretionary structure, but from
numerous examples it seems to be demonstrated otherwise. The appearances are similar to
those presented by a semifluid mud, or any viscid body flowing over a slightly descending
surface, or impelled along by some other force. A very analogous appearance is often pre-
PORTAGE GROUP.
233
There seems at least no other mode
There is a thin coating of shaly matter upon the surface, and the
whole appears to have been moved along while in a semifluid state, either from some force
applied, or from the inclination of the bed of the ocean.
The surface of the ice presents all the inequalities of the flowing water,
of explaining these phenomena.
Another analogous appearance is to be seen in the cooled cinder from iron furnaces,
which presents all the inequalities of the first and the congealed streamlets which have flowed
for a few inches over the surface.
The woodcut below is a facsimile of a layer of shaly sandstone taken from the bank of the
sented when a small stream or rivulet, oozing from a cliff or descending a steep hill, becomes
and occasionally little streams have broken through, and flowing a short distance have become
suddenly frozen.
Genesee near Portage.
frozen.
：
¿
șÀ
№è
Zaezzº»
≡ Ø%%%%%%
żżğźğģ
§§¶ （×）~tº
：
（）
Ņ
№
È）
\È
}§§
！ №.
W
！
§}\\§§§
！§§
§§ae
¿№Ă（**）Ņ
§.••• • •Å
，∞
ĻĶA
§
ÈŅ
§È
§§
&
№ŅŠŇ\\§^
RŅŅŠŅN\\§§
*§§§§*ºſº-
�RNÒ\\Ķ
\，}{ſ}
----►§§№.ºs）
）;§），&&\\§ſae
،§SNÈ™)¿ŅĶ：
§è.S. №§§
S**，*\ſ*ºš ،}
§3
Ņ\
sae
ŅŅĶ%
№ſ,
№
*\
È
SNĘ
`\\
\\
§§№ſ.{
§§§ ،：
§§ Ģſaevºae$（）;\}
$（'\\\
Ņ|}
E:
==#
Éx?
:=º:
3.
=º:
\\
|
:
ſ.|-
3
#3
\！\！
|
\\
T
: º
===
E: E
2:#
É
à
|
|
|-
-:
º:
\，|- ， ：
\ \ \ / |
\\||||||||||| ：||||||||||||||||ſå}\\|ſå
SOE .№， ſ
||
Many of them
Cast of flowing mud, Portage, N. Y.
30
There are several other similar appearances, all varying in some degree; and as we would
[GEoL. 4th DIST.]
naturally expect, no two localities present precisely the same form of surface.
appear to have been casts in previous depressions, as if the fluid mud had filled inequalities
hollowed out by the action of flowing shallow water over a muddy bottom. The ripple-
234 - GEOLOGY OF THE FOURTH DISTRICT.
marks and mud-cracks both indicate a shallow sea, and these surfaces often offer equal
evidences of the same. It frequently happens also that in the same layer presenting these
casts of flowing mud there are diagonal lines of lamination, indicating the power and action
of currents upon the transported matter, being another fact in proof of the shallowness of
the sea. -
Many other illustrations might be given presenting the same general character, and in
none of them is there any appearance like the Ordinary concretionary structure. From nume-
rous examinations of this kind, I have been led to the conclusion that these are due to the
cause here assigned. Having seen no description of anything of this kind, I have been under
the necessity of attributing them to some cause; and if this be not the true one, I shall be
glad to embrace any other view which will more readily and naturally explain them.
Casts of Mudfurrows and Stria.
I have applied this term to certain appearances upon the under side of the strata of sand-
stone, or flagstones, which are numerous and extensive in the Fourth District, as well as
elsewhere in this group; having from my own observation detected them in other parts of
New-York, in Pennsylvania, Ohio, and even to some extent in Indiana.
These casts are elevated lines or ridges upon the surface of the stone, varying from the size
of the usual scratches upon the present surface of the strata to the diameter of half an inch,
and even one, two and three inches, and in one case I have seen a specimen six inches in
diameter. -
The only assignable cause for these ridges is the action of a current flowing over the sur-
face of the strata, sometimes transporting sand and at other times coarser materials, which
furrowed the surface upon which the subsequent deposits were made. They are, in all cases,
preserved upon the under surfaces of sandstone or shaly sandstone layers, which rest upon
soft shale, so that the furrows or scratches must have been made in this mud. They are not
all confined to one position, but appear at different depths in the group; showing that the
cause, be it what it may, operated through a long period, and in a pretty uniform manner.
The ridges are never curved or bent on one side; and though two systems are sometimes
observed crossing each other, they are still as well defined and their course as unbroken as
in the glacial or alluvial scratches upon the surface of the present rocky strata.
From the frequent occurrence of these, and their continuation through a great thickness of
strata, we can hardly suppose the furrows to have been made upon hard surfaces; and if we
suppose the mud in which they were made to have been soft, it seems almost impossible to
conceive how they should be preserved. Still the numerous similar facts in other rocks.
prove that even the most delicate markings are preserved, under even more unfavorable cir-
cumstances. The tracks of birds and reptiles in the new red sandstone, with the impression
of rain drops, is equally difficult to comprehend, were it not demonstrated beyond all question.
Again it has been shown that in the Medina sandstone” the delicate wave lines and the minute
* Pages 52 and 54 of this volume.
PORTAGE GROUP. 235
ridges of sand, piled up before some little obstacle in the current, are preserved with the
same integrity as they appear upon a sandy beach just left dry by the receding tide. In the
same manner, the evidence of these slight scratches and deeper furrows in the mud of the
Portage group have been preserved in the casts formed by the succeeding depositions.
Nothing can be more clear and convincing than the proofs, and nothing more beautifully illus-
trative of the effects of oceanic currents upon the bottom. We have little space here to
describe these phenomena, and they should be seen to be fully appreciated. This fact, how-
ever, may be added to the number, if we have not already sufficient, to prove the condition of
the sea in these remote periods. -
The following woodcut represents a surface where three systems of ridges appear, or where
the grooves were made in three directions. - .
102.
|
Ø:
º
ºftºft
% 22.2% *
- à #
223:
* = * *
Casts of Striae—natural size.
30*
236 GEOLOGY OF THE FOURTH DISTRICT,
This specimen is from Erie county, not far from the lake shore, and in the same locality
numerous others were observed at different heights in the strata; some of them were much
larger than those here represented. In two instances where I carefully noted the direction of
these ridges, it was nearly E. and W. This is subject to a few degrees variation, but I have
found the same general direction to prevail over wide areas.” In some instances the furrow
appears to have been made in mud which was partially indurated, and the cast presents the
same appearance of a tremulous motion in the body making the furrow, which is sometimes
observed in the alluvial grooves. In many of these casts the angles are sharp, as if the
grooves were made with a pointed or angular body; in others they are round, as if the body
were smooth, or the mud partially flowed together before the period of the succeeding de-
position. -
In many instances the striae are not coarser than those of common alluvial or glacial origin.
In Seneca county these striae occur upon the surface of a dark colored argillaceous sandstone,
which rests upon a sandy shale of a blackish color. The shale is so friable that nothing is
preserved in it, but the surface of the rock above is thus striated. This case is peculiar,
and I think I have detected the same stratum similarly marked, at the distance of twenty
miles. It appears in the ravine at Goodwin's falls, on the eastern side of Seneca county, and
on the western side of the county near the head of the lake is a similar stratum. The posi-
tion of the two is almost or precisely the same, while in lithological character and the mark-
ings no one can distinguish the difference. Thus it appears that, whatever may have been
the cause, it operated very uniformly over large surfaces.t - a
It will be recollected that there are no uplifts or disturbances which could refer these
markings to the sliding of one stratum on another; and besides, they are always found at the
junction of argillaceous with more arenaceous strata, the former of which could not make an
impression in the harder stone. Many of them are so large, and their direction so uniform,
that this cause could not have produced them, even allowing evidence of its operation, which
does not exist. - - w
In some instances these ridges can be traced for a few feet in extent only, one end being
large, and gradually disappearing as if the furrow was made by some heavy body striking the
bottom for a short distance, and then lifted above it. Sometimes the ſurrows appear to have
remained unfilled for a length of time, from the fact that they are then partially filled with
drifted shells, of which the following is an example:
er-
* Some ridges of this kind have since been examined on Cayuga lake, which had a direction N.W. and S.E. It is often
extremely difficult to ascertain with accuracy their direction; for being on the lower side of the strata, it is only where we
can find an overhanging rock that they can be examined, and we cannot always be sure that it may not have been slightly
moved in its bed. -
# In this instance, although large surfaces were examined, the stria, have all a single uniform direction.
PORTAGE GROUP. 237
N
ºº
N:;
§
M -*** . .º.º. º. º. º
S esse- . . Łs-BR ==E
|S º º 7 : f. Eºſ | Fº
º N - Wº ɺ |% I
º §§ - § \; sº | s: º- ºft §
§§ ;#sº
§§ - %& §=########3:#E===#.
º §§ ==3% ji=#:#: * * * ,
§ #º: §
;
a Fæ
:=ºjż==%;
#ſº
§ āşş
§§§ºś. ÉS #º
§§§ %. Pºe ääß 5:= º - .*
§º ==Re--
§§§ EFº: E3:# : É=###!º
§§§º:#######################
§§&############## ==#E=E= --------
§ Wº * Es:
$SN: Nºs:
- :=>==
º:
º: : º
- >:
º - * - ### º-ºº- === -E--->
Nºr-E É== E: E: EEFº.º.
- §:E::::::==#EE: = z = z º. ºr a º :=#Egy, º,
º ££:######5~ % 2.2 g º ºr 22 ź% -
N - # % % Zºº.2.2 %
Cast of Mud-furrow, with Shells.”—Natural size.
This cast has upon its surface the marks of numerous shells, all of single valves, which
appear to have been quietly floated along over the even surface, till they lodged in the de-
pression from which they could not be removed. The succeeding deposition covered them,
and they became attached to it, and it now appears as a cast in relief. Upon the lower surface
of the layer from which the ridge rises, there are no shells, though they are quite numerous
on the ridge. .
Many other interesting illustrations of similar kinds could be given, but these appear suffi-
cient for the occasion, and to show their origin, which proves at least some interesting facts
in relation to this period. -
Localities. – Almost every ravine and stream upon the elevation which rises to the south
from the Hamilton group, exposes the rocks of the Portage group in greater or less perfection.
Along the banks of Cayuga and Seneca lakes, towards the southern extremity, these rocks
form cliffs, often of considerable height, which, from the alternating hard and soft layers and
the numerous vertical joints, present the appearance of solid walls of masonry in distinct and
regular courses. Isolated masses, like some huge column, are often seen standing out in bold
relief from the line of the cliff, being the remains of a previously exposed surface which has
crumbled away. -
* It must be borne in mind that the upper surface, as represented, is the lower in nature.
238 GEOLOGY OF THE FOURTH DISTRICT.
At Penn-Yan, in the outlet of Crooked lake, and in the ravines of the neighborhood, the
shales and shaly sandstones of the group are well exposed. The Cashaqua shale here em-
braces thin courses of sandstone, and contains numerous fossils. Along the shores of Crooked
lake, and in the ravines entering it, and at Hammondsport, its southern extremity, the rocks
of the middle and higher part of the group are well exposed. They are everywhere known
by the thin flagstones, covered upon their under surfaces by the short rigid stems of Fucoides
graphica (see woodcut, page 241). At the southern extremity of Canandaigua lake, and in
the deep ravines which extend from the valley of the same in the vicinity of Naples, the whole
group is fully exposed, and these places offer good points of examination. The small lakes
to the west of the Canandaigua, viz. the Honeoye, Hemlock and Canadice, with the ravines
extending from them on either side, are all good points of examination.
The Caneseraga creek, and its branches in the vicinity of Dansville, offer good exposures
of the rocks of this group. t - - -
The small streams flowing in the Genesee valley between Dansville and Mount-Morris, on
both sides, afford good opportunities of investigation. The Cashaqua creek (see illustration,
page 226), is the best of these. - * p -
The Genesee, as before noticed, in its passage from Portage to Mount-Morris, exposes the
whole series of rocks in fine mural escarpments which rise from 50 to 350 feet high. The
examination of this gorge throughout its whole length, will give a most perfect and connected
view of all the subdivisions of this group. . - - -
West of the Genesee, the valley of Allen's creek, of the Tonawanda creek, and the lateral
ravines of the same, expose these rocks in a very perfect manner. The branches of Cayuga
and Seneca creeks in Erie county give an exposure of the group throughout. i
The shores of Lake Erie, from Eighteen-mile creek to the State line, are composed of rocks
of this group, presenting themselves in cliffs of 20 to 100 feet high. The streams and ravines,
particularly the Canadawa, the Chautauque and the Twenty-mile creek, also give good ex-
posures of this group. The deep gorge of the Chautauque creek not only exposes the rocks
of this group, but their connection with the Chemung group, as well as the rocks of the latter
through several hundred feet in thickness, $
Finally, scarcely any stream or ravine which flows over this group can be examined, with-
out finding a good exposure of some portion of the strata.
Thickness. – The thickness of this group on the Genesee cannot be less than one thousand
feet. The fall in the river from the head of the falls to the base of the group near Mount-
Morris, is nearly six hundred feet.* The rocks rise about two hundred feet higher; and the
dip in this distance of ten miles in direct line cannot be much less than three hundred feet,
allowing for undulations. r - : -
The rocks of this group extend along the shore of Lake Erie for about thirty or forty miles,
before coming to the mouth of Chautauque Creek. In the banks of this creek there are about
* See “Topographical Sketch of the State of New-York,” in Transactions of the Albany Institute, p. 97.
PORTAGE GROUP. 239,
three or four hundred feet of thickness exposed, which, together with what is exposed on the
lake shore, makes the aggregate thickness little less than fourteen hundred feet.
From the great breadth of surface occupied by this group, if the dip southward were uniform,
its thickness would be much greater than here estimated; but it is evident, from numerous
observations, that there are undulations which materially affect any calculations based upon
the dip of the strata. By carefully examining the best natural sections, it appears that the
average dip is about twenty-five feet in the mile; though in many localities, and indeed the
greater number, the amount of dip is twice as great as this. In these cases, however, no
account of the undulations is taken.
Minerals of the Portage group.–The concretions contain crystallized carbonate of lime,
and sometimes sulphate of baryta. Iron pyrites is freely disseminated through the rock; and
from its decomposition, the surface of the slaty laminae and the sides of joints are often stained
with iron. It also gives origin to sulphate of lime or gypsum, which often coats the shaly
laminae, or appears in the form of small crystals in the seams and joints of the same. Car-
bonaceous matter is disseminated through the black shales, and sometimes appears in seams
of half an inch thick. Some fragments of large vegetable forms appear, and thin laminae of
coal usually accompany these. From the frequency of these small seams of coal, which are
usually of no greater extent than the specimen procured, excavations and borings have been
undertaken in search of larger beds. It is unnecessary to say that these always fail, as do
all similar undertakings in rocks of this period. It is, however, impossible to prevent such
useless expenditure of time and money, except by some source of information which can meet
every one, and which shall find its way to all parts of the State.
Springs. – The country underlaid by the rocks of this group is well watered by never-
failing springs. It must be remarked, however, that the practice of indiscriminately clearing
the woods from hills and valleys will in time operate injuriously on the surface, by drying up
those sources which now supply the pure and healthful springs which water the surface, re-
freshing both to man and beast. Except where the black slaty shale is thick, there is no
difficulty in procuring water. In such instances the vertical joints appear to be more open,
and to allow the percolation of water through the mass. There is here no remedy but to
bore through the black to the green shales, which are less divided by joints, and usually
impervious to water. In the present state of the country, however, there is little difficulty in
procuring the desired supply, and that with little labor or expense. If the true origin of springs
was known, and the means taken to protect them, there need never be wanting a sufficient
supply of water on the surface. By the present practice, however, of cutting the wood from
the higher grounds, many of the springs and smaller streams will eventually be dried up.
Agricultural Characters of the Portage Group.
In some parts of the country occupied by this group, we first notice a deficiency of calcareous
matter in the soil. This change is indicated by a different growth of timber, and a correspond-
240 GEOLOGY OF THE FOURTH DISTRICT.
ing change in the products of the cultivated soil. Wheat does not always prove a sure crop,
after the field has been cultivated for some years. When first cleared, the land produces
good crops of all the grains. In this statement, however, must not be included the valleys
and the low northern slopes, which are deeply covered with northern drift and alluvium,
containing a large proportion of calcareous matter. This on examination proves to be com-
posed of the ruins of the limestone and calcareous shales before described, with a small ad-
mixture of sand.
This kind of soil is but sparingly spread over the higher grounds, and in many of the highest
places is not known at all. In consequence of its absence, the character and productions
of the soil of the valleys and of the hills are quite different. $.
The soil derived from the lower part of the group is a stiff clay, the sand being in too
small proportions to produce much perceptible effect. As we ascend, the arenaceous matter
increases, and the broken fragments of the sandy strata become intermixed with the finer
materials, giving it the character of a clayey gravel. The fragments, however, show little
effect of attrition; and from being flat and irregular, the soil is known locally as “flat gravel,”
to distinguish it from that of the valleys, where the fragments are rounded into the form of
pebbles. •
In the valleys and on the low northern slopes of this group, the soil produces wheat with
the same facility and equal certainty as the formations north of it. As we ascend to the south,
the wheat crops are less abundant and less certain, and this gives place to the coarser grains
and to pasturage. For the latter object, the soil is superior to that on the north of it, and the
evidence is fully substantiated by the increasing number of cattle and the produce of the dairies.
Without knowing any thing of the charācter of the soil or underlying rocks, the observer
cannot fail to notice this great difference in the products and in the appearance of the farms,
and the absence of the northern drift marks more strongly the distinction as we progress
southward. The soil overlying all the groups as far south as the Tully limestone, whether
it be clay, gravel or loam, presents one general character, viz. that of being highly calca-
reous; but after we leave these formations, we soon become sensible of the change ; and
although the same external characters of soil are presented, yet from the absence of the
calcareous ingredients, it does not produce the same vegetation naturally; and neither will
the skill of the cultivator enable him to do so for any considerable time, unless he supplies
the matter which is wanting.
It will hereafter be shown in what manner these soils may be benefited by the application
of certain manures, with the means and places of obtaining them. It is, however, very ques-
tionable whether any improvements rendering these soils capable of producing permanently
good crops of wheat, will render them more profitable, or enable such farms to compete
successfully with well stocked farms. - -
At present the occupants of farms of the southern tier of counties have many difficulties to
contend with ; the land in the first place is heavily timbered, and when this is overcome, it
is found difficult to procure good stock. In many instances, and perhaps the greater number,
the farmer has not the means of clearing and stocking his farm at the outset, so that he is
|PORTAGE GROUP. - * 241
continually laboring under difficulties, which are only surmounted by years of patient industry
and economy. -
We may look forward, however, to a different state of things: in a few years more, this
portion of the country will wear a different aspect; the improved breeds of cattle and sheep
will place the owners of the grazing farms in a position of equality with their usually adjudged
more fortunate neighbors upon the wheat-growing soils; and the strong arms and manly fronts
that have borne the toil and exposure will reap the harvest. -
Organic Remains of the Portage Group.
The paucity of fossils in this group, when compared with those below and above it, is one
of its most striking characters. Whole days may be spent in searching, in some parts of it,
without finding more than a few, and perhaps even no shells. In a few fortunate localities,
some forms have been detected which seem peculiarly typical of the group, and, so far as at
present known, have never been found elsewhere. They are not only specifically unlike,
but some of them even generically different from any that have been seen in the other groups
in the district.
In this absence of fossil shells, we have a great abundance of marine vegetation, or fucoids,
and these are very characteristic of the group. Scarcely a locality can be examined, where
one or more species does not occur. -
The following woodcut illustrates the most abundant form, and one which everywhere
marks the central portion of this group :
ſº
**
º
š
|
S.
===s*=E=-
Fºº-º-º:
sº- § §ss==S || ||=s=Esºs
$ESS §s:#Es S ſ Eºsi-ºº:
. ===
Eº º º-º-º-º-º-º-º-º-º- *
g- | É=== -
Essº
§:#=te:S:
o ===S
§§
ºw- Sºsº-t:S
ESEs
Eš= ====
b- - --
H------
Łº
E.
E
E::=#:
s== ==Eº: -
-º-º-º: ====
E--->
> Sis: ...:
Sºsº-º:
Fucoides graphica
Geol. 4th Dist. 31
242 " GEOLOGY OF THE FOURTH DISTRICT.
This fossil occurs in short rigid fragments, lying in great confusion, spread over the sur-
face of the thin flagstones of the middle part of the group. It is only by its general form and
the arrangement of the fragments that it can be characterized. It can be found in all localities
of the flagstones, and, from the extensive use of these, it may be seen on the sidewalks of all the
villages upon or near the group. Some of the finest specimes I have ever seen are used in
the streets of Geneva, and the numerous little ridges upon their surfaces will be recollected by
every one who has been in this village. At Penn-Yan the same character is presented in the
flagstones, but less perfect than at Geneva. * .
Almost all the thin sandstone layers present this appearance, and the beds of the ravines
are strewed with them. - -
This species of fucoids disappears towards the upper part of the group, where the sand-
stone becomes thicker and in greater proportion, and gives place to another species. This
consists of small round stems, extending vertically through the strata, as if they were growing
at the time the sand was deposited around them.
105.
º
#j
ſº-
º-ºº:
ąsº-ºº:
s:
s:
Ess:=
º::==
fife:=#E=
sº
ğ
§:==
N:=
===
:#E
- --- Še 2.
N== ::\Sº;
Nº É=#E= Sº-ºº:
&- . === #E
§§
º ë : , S: ---E -º-º-º-º:
ºsłºś
º § £º: ####### º s
wº- º EÉs. * . ===:=$$$ºs º º
& l *=$#$ºs=#
W *-i-º-º-º-º-º:
§ §§ º
Eaº $ºse=s==
ºs-ºº:Éjºš
3:=-
|
|
º
{ És
| És:
Áº, § º § § § §§§
ſº a y | | | | | ||
s:
Fucoides verticalis.
This species has always been found characteristic of the upper part of the group; and
although in the higher rocks there are sometimes vertical fucoids, they never present the same
character as those of Portage.
It may be seen at the Lower falls of Portage, and in many of the sandstone strata above
this; but it is most abundant in the upper sandstone at Portage, and the terminating mass of
the group is everywhere known by its presence.
PORTAGE GROUP. 243
In the Cashaqua shale, or lower member of this group, there are several species of shells
which have not been seen in any other rock, and at the same time there are no fossils found
with them which are known in other rocks beyond the group.
The following woodcut presents the more common forms:
106.
§º
$ºſº
|
:
*
ºs- .
E=-3-º
º
Wº: ź % ſº \ º §§
sº
Ž º
4/miſſiſſiſſiſſilſ
|
§
5. ºf
% :
%
1. Avicula speciosa. 4. Orthoceras aciculum. 7. Pinnopsis acutirostra.
2. Ungulina suborbicularis. 5. Clymenia'ſ complanata. 8. Pinnopsis ornatus.
3. Bellerophon expansus. 6. Goniatites sinuosus.
1. Avicula speciosa, n. s. – Semioval or semicircular; hinge line straight, extended beyond
the width of the shell, and angulated at either extremity; surface marked by about ten ribs,
which are crossed by beautifully curved concentric lines. - -
1 a. A specimen presenting both valves, attached at the hinge. This is not an unusual
condition of this fossil.
The shell is usually very minute; its markings are very beautiful, and easily recognized.
It is quite abundant in the Cashaqua shale, and alone seems sufficient to identify the mass.
Locality—Cashaqua creek; Genesee river; Penn-Yan; Eighteen-mile Creek.
31*
244 - GEOLOGY OF THE FOURTH DISTRICT,
2. Ungulina suborbicularis, n. s. – Shell suborbicular; surface marked with fine concentric
striae, and a few stronger folds; beak rather prominent.
This fossil is not uncommon, but imperfect specimens are usually found.
Locality—Cashaqua creek; shore of Lake Erie.
3. Bellerophon eaſpansus?—The spire is wanting, and this imperfect specimen, presenting
the expanded bilobate lip, is all that has been seen in the rock. It closely resembles the
figure of Murchison, pl. 5, fig. 37.
4. Orthoceras aciculum, n. S.–This very delicate and beautiful species is usually re-
placed by iron pyrites, and so much destroyed as to be unfit for a figure. -
Locality—Cashaqua creek.
5. Clymenia? complanata, n. S.–Flattened involute; whorls numerous, crossed by nu-
merous slightly raised striae, which often appear undulated.
This fossil always occurs replaced by iron pyrites, and more or less decomposed. It is
provisionally referred to the genus Clymenia, its structure not having been satisfactorily
ascertained. -
6. Goniatites sinuosus, n. S. – Discoidal, usually somewhat flattened, rapidly expanding
from the first whorl; volutions crossed by unequal undulating striae; septa sinuous.
The specimen figured is a fragment; there is a perfect one in the State Collection, mea-
suring four inches in diameter. -
Locality—Cashaqua creek, with the two last; also Lake Erie shore.
7. Pinnopsis" acutirostra, n. s. – Sub-cuneiform ; surface marked by about twenty-six
diverging ribs, which are crossed by numerous faint undulating lines, and a few stronger
wrinkles of growth; beak extended, acute and slightly incurved. . -
This is one of the peculiar forms of this group, and apparently referable to no established
genus. - -
Locality—Cashaqua creek.
8. Pinnopsis ornatus, n. s. – Obtusely cuneiform; surface marked by more than forty
diverging ribs, which are crossed by beautifully arched striae.
The specimen is slightly imperfect on one side. - -
This and the preceding species occur together, and from their similarity, are not often dis-
tinguished; the number of ribs and the form of the shell are, however, sufficiently distinctive
marks.
Locality—Cashaqua creek.
* This generic name is proposed for the two fossils here figured, from their resemblance to the Pinna.
PORTAGE GROUP. 245
The specimens illustrated in the following woodcut occur in the more central or higher
part of the group, being unknown in the Cashaqua shale, except No. 9.
107.
*E.
E.#
º
§:#$: ##########
* º- Sºº-ºº
3S3:S: #=#################
:S→ º 2::$3:Eºs:->
Sºś ##########
E: ES: º: :3:
º: £=#3; É==
º
7. Bellerophon striatus.
1. Delthyris laevis. 4. Lucina'ſ retusa.
2. Cardium ? vetustum. 5. Nucula lineolata. 8. Goniatites bicostatus,
6. Astarte subtextilis. 9. Goniatites sinuosus.
3. Orthis tenuistriata.
1. Delthyris lavis, n. S.– Somewhat semicircular; surface smooth, or with scarcely
perceptible concentric lines, and sometimes a few strong folds near the margin; mesial fold
moderate, strongly impressed in front; beak prominent; cardinal area moderate; foramen
partially closed.
This is the only fossil of the genus seen in the district, which is destitute of ribs. It is
apparently limited in its range, being unknown beyond the borders of Seneca and Cayuga
lakes. The fossil is often much larger than the figure.
Localities—West side of Cayuga lake; Shore of Seneca lake.
2. Cardium? vetustum, n. S. — Somewhat triangular; slightly carinated upon the posterior
slope; ribs plain.
This fossil occurs in the soft green shale, usually presenting an obliquely triangular figure.
Localities—Cashaqua creek; Genesee river; Shore of Lake Erie.
246 GEOLOGY OF THE FOURTH DISTRICT.
3. Orthis tenuistriata, n. S. – Broad elliptical; beak small, rather prominent; surface
covered with very fine radiating striae, which are crossed by a few concentric wrinkles.
This is more finely striated than any shell of this genus in the district.
Locality—Shores of Crooked lake.
4. Lucina? petusa, n. S.–Obliquely suborbicular; beak small, oblique; surface marked
by concentric lines, which are much stronger on the anterior margin.
Locality—Shore of Lake Erie, in Chautauque county.
5. Nucula lineolata, n. s. – Obliquely ovate ; posterior slope straight; surface marked by
regular, equal concentric lines, which terminate upon the posterior slope before reaching the
margin of the shell.
Locality—Lake Erie shore in Chautauque county.
6. Astarte subtertilis, n. S.– Suborbicular ; beak prominent; surface marked by strong
concentric folds and finer lines, which are crossed by a few faint elevated radiating striae.
The shell is incorrectly figured. -
Locality—Lake Erie shore in Chautauque county.
7. Bellerophon striatus? (BRONN. PHILLIPs, Palaeozoic Fossils, pl. 40, f. 198.)—Sub-
globose, carinated ; “keel narrow, elevated ; surface marked by fine arched striae which meet
the keel in a slight retral angle.” Phillips. • *
Our fossil agrees precisely with this part of the description, but the aperture is less broad
than the figure of Mr. Phillips.
Locality—Shore of Lake Erie, Chautauque county.
8. Goniatites bicostatus, n. s. – Sub-globose or discoidally involute; umbilicus moderate,
very distinct; last whorl with a distinct subdorsal elevated line on each side; surface marked
by arched striae extending from the umbilicus and meeting the elevated line at an acute for-
ward angle, and receding from it on the back at a more acute retral angle.
Locality—Shore of Lake Erie, Chautauque county.
9. Goniatites sinuosus (Illustration No. 106, page 243). — Discoidal; involute; surface
marked by undulating striae.
This fossil seems reſerable to the species above, though the marks of septa are very in-
distinct. It is thus known to range from the Genesee river to Lake Erie. -
Locality—Lake Erie shore, Chautauque county.
The following among the most beautiful of the crinoideans in the system, occurs in this
group; the sculptured column and tentaculated arms and fingers place it among the most
ornamental forms of this family of fossils.
PORTAGE GROUP. 247
108,
º
||#|
|§Çſ:ſº§
É|}
:§W:&ºº%
.
W|º
Å º
\| º º § :
Wº; § | §§ †
§ § N ! º § § § ń - ; ; #
Wi. § §§ º |} º Will ài | º § §
º § § §§ º º #
{\º Wº §§§ lºſſ, W §
§ § §§ § º º |
º º #
§ º \\ § |N *Wu #
º ŠEŠ - º
jū [ \
1. Cyathocrinus ornatissimus, n. S.–Pelvic plates five, pentagonal; costals five 3 some-
what heptagonal; scapulars hexagonal. Arms in part proceeding from the scapula, and divid-
ing and subdividing into hand and finger joints, which are tentaculated. Column somewhat
pentangular above, becoming rounded, and the joints increasing in thickness below.
2, 3, 4 and 5. Portions of the column nearer the base.
This fossil occurs only in a limited stratum, upon the shore of Lake Erie, in the town of
Portland. Some fragments of columns were first found on the shore near Eighteen-mile
creek; subsequently a larger number were found farther up the lake, and finally these were
traced to the original stratum which is not more than six inches thick, and thinning out in
every direction within five feet of the centre. This stratum is composed almost entirely of
the columns of this fossil, closely packed together. They appear to have flourished in great
numbers in this favored spot, and to have been swept down suddenly, the whole forest
becoming inundated by a deposit of mud.
From the immense numbers of columns and the fragments of the superior extremity, there
must have been several hundred individuals living in this small space, and so suddenly and
completely were they overwhelmed that not a fragment appears to have escaped,
248 GEOILOGY OF THE FOURTH DISTRICT.
Localities of Superposition.
The junction of this group with the one above is nowhere so well defined as the instances
already illustrated. The terminating mass of the Portage group is usually a heavy thick-
bedded sandstone, marked by the presence of vertical fucoids. Above this we find shales
and shaly sandstones, differing in some degree from those below, and manifesting the presence
of Delthyris and Atrypa.
The channel and lateral streams of the Genesee above Portage present a continuation of the
series almost completely. The order is illustrated in the section passing through Allegany
county (Pl. xi.). The Portage sandstone is succeeded by olive shaly sandstone and shale,
and this by black micaceous slaty shale, with septaria; to this follow shales and coarse sand-
stones, with fossils of the Chemung group.
On Lake Erie the thick-bedded sandstone terminating the Portage group is succeeded by
coarse shales containing fossils of the Chemung group. This junction may be traced south
of Laona. Again, on the Chautauque creek the sandstone is scarcely defined, and there is
little change in lithological characters from one to the other.
At many intermediate points the change here indicated can be readily observed, but the
absolute contact of the two groups is rarely visible. - - •
The greatest development of this group, and the point where it is most distinctly sepa-
rated from the next above, is on the Genesee river. Although it is obviously marked farther
east, there does not everywhere occur the thick-bedded sandstone at the termination; and it
would appear from the investigations in the Third District, that there are not the distinctive
characters in the fossils which are so prominent throughout the western part of the State.
Again, as we approach the western limit of the State, we do not find the distinctive features of
the two groups so well marked. The lower part of the Chemung containing fossils typical
of that group, possesses more of the lithological nature of the Portage group than it does
farther east. Still farther west, where I have examined these rocks, in Ohio and Indiana,
there is a closer resemblance in the lithological nature of the strata of the two groups, and
the change is attended by a great diminution in the number of fossils in the higher one. In
this part of the country, no distinction has been made between different parts of the mass;
neither is it there of much practical importance.
The facts in relation to this group, and its connection with the one above, are not peculiar
to these, but appertain more or less to all our sedimentary deposits. The distinction, therefore,
between groups where the whole series is sedimentary, cannot be relied upon over extensive
districts; and all such subdivisions can be considered no more than those of convenience, which
in some places are strongly marked and readily identified, while in others the lines of de-
marcation are obscure, and the distinguishing characters fail in a greater or less degree.
Whenever we have an opportunity of comparing a complete tabular list of the fossils, with
their geographical distribution, we shall find, that what in one portion of the country are
limited in their stratigraphical range, are nevertheless in other places not thus restricted;
PORTAGE GROUP. t 249
\.
and we shall do well to bear in mind, what has been before remarked, that the conditions of
the ocean bed and the nature of the sedimentary deposits has greatly influenced the character
of the organic forms. It may thus happen that the fossils so typical of the Chemung group
commenced their existence in the eastern part of New-York much earlier than in the western
part; and, therefore, the strata equivalent in age to the Portage group may there contain
fossils which at the west appear only at a later period. -- - -
109. .
\º
W
\\\\\\\
º G
\ \\
[GEOL, 4th DIST.] - 32
250 GEOLOGY OF THE FOURTH DISTRICT.
º
º
|
*
ſ
% |
º
- sº º º W ! - º
ſº
% | º
}
º
º
º
tº.
º
ſº º 'ili %. %; º - ãº
sº §§ ==#sºft| | || || 'ſ fill I ºff f' |\ſſ|| w ຠº §§§
ºfts šš/) || || || '1/ſº § |||ſº % Wº
i. #| || || || ||_2% . - , Illil. , * żºš
º §§ ſº W f - º, 23.2% ºr ºS$º
º i º Š §
ºš 3 tº: *. g|||}| º ºft
wº º
º :*=== =#:###==º ##########3
| #: Ét cº-º-º-º-º-º: Rº: ~ É ==5A §
*==-º-º-º-º-º-º-º: sº- ºr z=º
Fall Creek, near Ithaca. From a sketch by Mrs. HALL.
Ithaca Group.
In the annual reports, this name was adopted for designating the highly fossiliferous shales
and shaly sandstones, so well developed at the inclined plane of the railroad, and on the Cas-
cadilla and Fall creeks, near Ithaca. Subsequently an examination of the highly fossilife-
rous strata along the Chemung river, and particularly in Chemung county, resulted in the
adoption of that name as designating this portion of the system. -- *
Succeeding examinations satisfied me of the identity of the formations at Ithaca with those
of Chemung, and this opinion was advanced in the annual report of 1841.
The reasons for merging the two in one, were stated to be the impossibility of identifying
them as distinct by any characteristic fossils. The same opinion is still entertained, after a
full examination of the strata, and a comparison of the fossils collected here and elsewhere in
well authenticated localities of the Chemung. There is scarcely a fossil known at Ithaca,
which is not found at numerous other localities; though it is true, not only of Ithaca but of
many other places, that some of the fossils are confined to the single locality in which they
OCCUIT,
By careful and extended examination, the Chemung group may be subdivided locally, where
it is most perfectly developed; but these divisions will hold good only over small districts of
country, position and lithological character having had much effect in producing these dis-
tinctions dependant on fossils. Examples of this kind will be noticed under the description of
fossils. .
CHEMUNG GROUP. 251
sº
ſ
\º § º
º º
º º t
ºiſº 6
[. º |E º |
ºśl. º º: §
iº
º º ſº
sºilº
º º
ſº
§§
|
&= -
§§
ºlº.º.º. §:=
º:=<=
Šºš
w º 3:2;5:=º
& Jºº-yº º:
Wº: tº: 3:23:2 º ‘. Ż
º: º zºº ...Arºº
#º &º
º *
s:-3
Chemung Narrows. From a sketch by Mrs. HALL.
28. CHEMUNG GROUP.
Including the Ithaca and Chemung groups of the Annual Reports.
(No. 9 of THE PENNsylvania survey.)
[See section, Plate VII, and R of woodcut, page 27.]
This group consists of a highly fossiliferous series of shales and thin-bedded sandstones,
sometimes in well-defined and distinct courses, and an infinite variety resulting from the ad-
mixture of the two ingredients. Except in a few localities, there is no very strongly marked
line of division between this group and the one below. The distinction consists in the pre-
sence of numerous fossils and the coarser grained sandstones, which are usually more impure
from argillaceous admixture than those below. Its lithological characters, however, are va-
riable; and though well marked across a single line of section from north to south, still another
at a short distance east or west of this presents considerable variation. -
These rocks, however, can everywhere be described as a series of thin-bedded sandstones
or flagstones with intervening shales, and frequently beds of impure limestone resulting from
the aggregation of organic remains. The whole series weathers to a brownish olive, and even
the deeper green of the shales assumes this hue. -
The shales vary in color from a deep black to olive and green, with every grade and mixture
of these. The sandstones are often brownish grey or olive, and sometimes light grey. More
32* .."
252 GEOLOGY OF THE FOURTH DISTRICT.
generally, however, there is a tinge of green or olive pervading these strata. Towards the
upper part of the group, in many places, there is a tendency to conglomerate; and in a few
localities the mass becomes a well-characterized puddingstone, still retaining the fossils of the
shales and sandstones. This conglomerate nowhere attains sufficient thickness or importance
to merit a distinct description; but in hasty observations it may sometimes lead to erroneous
inferences, since it resembles in many respects the distinct and well-defined conglomerate
which rests upon this group in the western part of the State, but which is totally distinct from
the same. -
Many of the shaly sandstones and shales of this group are highly micaceous; and towards
the upper part of the whole, the shales are reddish, coarse and fissile, with much mica in
small glimmering scales. There is also in these shales a slight change in the character of
the prevailing organic forms. - • ... •
From being well developed along the Chemung river at numerous localities, and particularly
at the point represented in the woodcut at the head of the group, this name has been adopted
for its designation. - - -
These strata rise to the south from the Portage group, forming the higher elevations of the
southern counties, and covering nearly the whole surface of the same. The greatest elevation
of these hills is about 2500 feet above tide water, and from 600 to 1000 feet above the deepest
valleys of the surrounding country. -
The outline section crossing this part of the State from east to west (Pl. 12), will give an
idea of the general contour of the surface. The deep valleys are bounded by abrupt hills,
while the surface between them is, for the most part, but moderately undulating. This feature
of the surface is entirely due to denudation, the valleys being all produced by this cause, and
the slight undulations in the strata have scarcely affected the surface in any perceptible man-
ner. The evidence of the denuding action is often plainly visible in some of the harder strata,
but the perishable nature of most of them has obliterated all traces of this kind. An inspec-
tion of the sections crossing these counties in a north and south direction (Plates 9, 10, 11
and 12, as well as the outline section), where the comparative elevations are given, will suffice
to give an impression of the vast amount of material removed. The outliers of conglomerate
resting on some of the higher hills of this group also prove the same fact, and show how
powerfully and effectually this agency has operated. An inspection of the map also shows
numerous points of the same, often with broad and deep valleys between them. In the val-
leys in this group are some of the highest lakes in the country; these will be noticed in
another place, with their elevations. w
The numberless natural sections along the deep ravines and river channels afford good
opportunities of studying this group in all its various developments throughout the district.
In many situations, its relations to the groups below can be distinctly traced in an almost
continual line of section from the Hamilton group upwards. Its relations with the rocks
above it are not so clearly seen in many localities within the State, but they are sufficiently
so for satisfactory investigation, and localities beyond the limits of the State present the same
order in the most conclusive manner. -
CHEMUNG GROUP, 253
The lower beds of this group are well exposed a little south of the head of Seneca and
Cayuga lakes, and at some distance above their level. The broken margins of the northern
escarpments, along the whole extent of the district, present good exhibitions of the same ;
while the water courses along the southern border of the State expose the higher beds, and
their connection with the rock next above. . -
This group requires to be studied at several localities, in order to understand the variations
in lithological and other characters which it undergoes in its extension westward, as well as in
passing southward toward the upper termination of the same. ... - -
Along the eastern margin of the district the strata are, as a whole, darker colored, with
more frequent intermixtures of the shales and sandstones, which less often appear in distinct
and well-defined beds. The shales are of a dark olive color, and the same for the most part
pervades the sandy strata, and it is only toward the southern border of the State that well-
defined courses of black shale are found. As we go westward, this character continues in a
greater or less degree, and there is little change along the sections from the head of Seneca
and Crooked lakes southward. - - - - - -
On the Genesee river we find the limits of the products better defined; the shale often in
thick beds, of a bright green color, and scarcely interrupted by sandy layers. The sandstones
at the same time are purer and of a lighter color than those farther east, and less intermixed
with shaly matter. Several subdivisions can be recognized along this river, which, however,
are not as clearly defined elsewhere. - - ( r
The following section presents the order and character of strata in this line of section:
112.
I. Portage sandstone, 2. Olive shaly sandstone. 3. Black slaty shale, with septaria. 4. Green shale, with grey sandstone.
5. Grey and olive shales and shaly sandstones. 6. Old Red sandstone. 7. Diagonally laminated sandstone and
conglomerate. *- -
On going westward from the Genesee river, there appears to be a constant augmentation in •
the quantity of the green shale, which is often the predominating rock; though from weathering
to an olive color, it does not always appear as distinctly. The sandstone strata become less
perfectly defined in general; though in several places in Cattaraugus county there are some
thick masses of greenish grey sandstone, very durable, and readily quarried into large blocks.
In the ravines in Chautauque county, extending toward Lake Erie, the shale still retains
its green color; the sandstones are for the most part thinly laminated, and partake of the color
of the surrounding shale. The dark olive sandstones, like those of Painted-post and other
places in Steuben county, which are thick and important masses, are recognized in Chautauque
county only as thin layers of brownish sandy shale containing the same fossils as farther east.
254 GEOLOGY OF THE FOURTH DISTRICT.
This thinning out of some portions of the group is not fully compensated by increase of some
other parts, (the green shale;) and there is an evident diminution in thickness, and a constantly
decreasing number of fossils, many species which are common farther east having disappeared,
while scarcely any new forms are seen. Fossils, however, are numerous in many localities,
and the same general appearance in their manner of aggregation and imbedding is preserved
throughout. - - 1 - -
Besides the general diminution of sandy matter and the absence of the brownish sandstones,
the red sandy micaceous shales have not been recognized; and they are nowhere visible in
the ravines west of the Genesee river, so far as observed. - - -
The frequent alternations of shales and sandstones, the interlamination and mixture, all
prove the operation of similar causes as in the group below. Although there is scarcely any
definable difference in the products of the two, yet we see an immense increase in the number
of species and individuals of organic forms. Judging, therefore, both from the condition of
the deposition and the nature of the organic forms of the two, the lower part of the Portage
group was deposited in a deeper ocean; and although there were numerous oscillations toward
the conclusion of the period, yet the conditions favorable to the production of numerous
species of shells did not supervene till after the final deposition of the Portage sandstones.
These remarks apply to the Fourth District; how far they are applicable farther east, I am
unable to decide. It is very clear, however, that as we progress westward there is a dimi-
nution of the Avicula, Cypricardia and allied forms, while the Brachiopodous fossils are at
first more abundant, and finally themselves diminish also. It is also equally plain that the
origin of the materials of this deposition was to the east of central New-York, and, probably,
to the southeast, as is evidenced by the thinning of the deposits, and the diminution of sandy
strata at the west. The increase of shaly strata in the same direction, which finally dimi-
mish also, proves the same; for this being longer suspended, was transported beyond the sand.
We have here a corroboration of the same view as presented under the Hamilton group, viz.
a position in eastern New-York, near the margin of this ancient sea, while towards the south-
west we approach that part of more profound depth and greater distance from shore. The
evidence continues throughout the Hamilton, Portage and Chemung groups; for in all these,
and the intermediate beds of shale and limestone, we find a constant diminution southwesterly.
There is also another fact of the same import, viz: In eastern New-York we find, both
in the Hamilton and Chemung groups, specimens of land plants, or such at least as did not
grow beneath an ocean. These are rare in central New-Y ork, one or two fragments only
having been found; and at the southwestern part of the State, and in Ohio, I have seen nothing
of similar character. The inference naturally follows, that these were derived from land on
the eastern margin of this ocean; and that some fragments floated westward, and were depo-
sited with the sand and mud. Many of the thin sandy laminae throughout the district are
often almost completely covered with small fragments of carbonaceous matter, apparently
derived from terrene vegetation. These seem to have been comminuted fragments of vege-
tables brought down by streams from the continent or islands on the east, and being spread
CHEMUNG GROUP. 255
evenly over the surface of the water, were distributed widely, and deposited with the sand and
mud. Similar deposits are going on in the lakes and in the bays of the ocean at the present
time, and it is a common occurrence to see the water of either covered with a thin scum of
comminuted particles of wood, extending for great distances. These appearances upon the
strata in New-York are seen in Ohio, specimens from the two being scarcely distinguishable.
All facts of this kind are interesting, as showing an approach to that period when terrene
vegetation flourished on a grand scale, and in its destruction gave origin to the great coal
measures of the United States. Throughout all the lower rocks of the New-York system,
there is no evidence of terrene vegetation, and consequently no proximity to coal-bearing
strata, and it is only subsequently to the deposition of all the limestone formations of this
system that this kind of vegetation appears. - .
The character of strata and materials composing the Chemung group can be illustrated by
a section or two, much better than by description. Hundreds of sections of the vertical cliffs
have been noted, but as they present little variation, a repetition would not be instructive.
The following is a section of the cliff at Chemung Narrows, from above downwards:
Feet. Inches.
I. Fissile olive shale, with Aviculae ------------------- -------------- 15 0
2. Compact shale, with Cyathophylli and other corals------------------- 0 6
3. Compact shale, with thin courses of sandstone separated by seams of shale. 13 0
4. Greenish grey sandstone, with seams of shale ----- ------------------ 10 0.
5. Greenish grey sandstone, with the weathered edges stained by oxide of
manganese and iron ------- ---------------------------- - - - - - - - 7 0.
6. Shale and sandstone, with Aviculae, Atrypae, and other fossils ---------- 5 0.
7. Soft greenish olive shale--------------------------------------- -. 3 0.
8. Compact sandy shale, with fossils --------------------------------- 2 0.
9. Shale in three distinct courses of 2, 4, and 6 feet --------------------- 12 0.
10. Corallines --------------------------------------------------- 0 2.
11. Olive shale, with abundance of fossils----------------------------- - 3 0.
12. Compact shaly sandstone ------------------------ ºs. º. º.º., º sº, º sº ºn tº tº sº wº - - 2 6
13. Shale with thin layers of sandstone, containing abundance of fossils------ 6 0.
14. Concretionary sandstone--------------------- -------------------- • 3 0:
15. Shale with thin layers of sandstone ------------ ams ass sm eme sm amas wºm. ------------- 8 0.
16. Below this to level of river, the character of rock not ascertained ------- 14 0.
This may be considered a specimen section, and gives the general character of the rocks of
the group in other places. The fossils of this place are chiefly Avicula pecteniformis, Stro-
phomena membranacea, S. interstrialis, Orthis interlineata, Delthyris prolata, Atrypa aspera.
Another section at Painted-post, in a different part of the group, presents the following
alternations from above downwards: -
256 GEOLOGY OF THE FOURTH DISTRICT.
Feet. Inches.
1. Sandstone, becoming shale farther south ------- --------------------- 6 0
2. Concretionary strata of shale and sandstone ------------------------- 5 0
3. Sandstone ---------------------------- ------------------------ 1 0
4. Shale, olive or brownish, and fissile ----------------------------- - - 5 0
5. Sandstone --------------------------------------------------- ... 1 0
6. Shale similar to No. 4 ------------------------------------------ 6 0
7. Thin stratum of sandstone.
* Shale-------------------------------------------------------- 4 0
9. Greyish olive sandstone 6 to 20 inches thick, running out and again re-
..” appearing.
10. Shale -------------------------------------------------------- 4 0
11. Brownish olive sandstone.------------- * * * * * * * * * * * * = * * * * * * * * * = ,---- 3 0
12. Shale, olive and greenish---------------------------------------- 2 0
13. Sandstone and interlaminated shale ----------------------- - - - - - - - - - 2 0
14. Shale -------------------------------------------------------- 7 0
15. Sandstone in thin layers --------------------------------- -------- 3 0
16. Shale -------------------------------------------------------- 7 6
17. Sandstone in thin layers ------------------- ------------ ---------- 5 6
18. Shale -------------------------------------------------------- 3 0
19. Sandstone in thin layers ----------------------- sºns tº ºs º me amº ----------- - 2 0
20. Shale-------------------------------------------------------- 2 0
The fossils at this place are Cypricardia, Avicula spinigera, Delthyris, Orthis 2
large numbers of Orthis unguiculus, Orbicula, Lowonema, Tentaculites, &c. Scarcely a
fossil is common to the two localities, though the lithological character is in a great degree
similar. Both the shales and sandstones are more deeply colored than at Chemung Narrows.
These sections are given from points where every inch can be measured, and consequently
there is no error respecting thickness or character; and as the whole is seen in connection,
there is no repetition of the same strata. At other places similar sections show some variation
from these in lithological characters, and also a considerable difference in the species of fossils
which the strata contain. We often find, in an exposed cliff of a few hundred feet extent, that
several of the sandy strata thin out, sometimes reáppearing, though often not again seen.
Such changes on a small scale are the same which the whole group undergoes in its western
extension, the evidences of which are already given. -
Diagonal lamination, and structure of strata. – The shaly strata of this group appear
to have been quietly deposited in the bed of the ocean, as we should naturally suppose of a
mass having its origin eastward. The sandy strata are constantly diminishing and disappearing,
and they present various interesting phenomena of diagonal deposition, interlamination, and
intermixture of shaly matter. The sand has evidently often been deposited at intervals, being
pushed along over the bottom covering a previously inclined surface; and this has been fre-
quently repeated. This character becomes more marked towards the west, where nearly all
CHEMUNG GROUP, 257
the strata present lines of diagonal deposition. This structure has been before illustrated,
under Medina sandstone and Portage group. *
Concretions, and concretionary structure of strata. – In the shales of the lower part of the
group, well defined concretions frequently occur in great numbers. These are highly cal-
careous, and present the common appearance of those in the groups below, being divided by
seams of crystalline calcareous matter, and contain cavities often partially filled with bitumen.
Towards the higher strata of the group, the shaly sandstone often becomes concretionary,
the lamina folding entirely or partially around a nucleus. These present various degrees,
being often nearly spherical, and becoming less and less perfect, till they present only strong
and abrupt undulations in the laminae of the stratum. Such structure usually occurs in the
micaceous shaly sandstone, and more strongly marked when such a stratum passes into shale.
The following section, near Painted-post, illustrates this structure: -
113.
as F- -
s= - : • zºº
Sºś - - \ asº. Sº ºftºº
- -- s § • Q ***--> sº - N - ~. , 2. ~ º - ** § §§ s sº
ššísº sº;
- -- - - - * > . § ºf *::::: - - - T- ~ 4. * :: S-> Fº
sºs Jº-Jº - Sº- *::- 1.7 ºrrº. - -- ~~ -
E---> --- - -**-ºsmº
Concretionary strata of shaly sandstone.
A similar structure is observable in the exposed cliff at Chemung narrows, and near El-
mira. The laminae of these concretionary masses preserve the same lines of division as where
the strata are plain, and they separate readily." *—
Spheroidal desquamation.— Fragments of the sandstone, of some parts of this group, after
weathering upon the surface, desquamate in concentric laminæ to the depth of the weathering.
This seems due to partial decomposition, which causes the separation, and obliterates the
lines of deposition. The blow of a hammer will often separate these concentric layers to the
thickness of an inch, while the apparent nucleus presents a different color, and the parallel
lamination of the mass is often visible. The influence of the weathering is very perceptible,
and is evidently the cause of the separation. -- *
Ripple-marks. – The thin-bedded sandstones and sandy shales of this group are often
ripplemarked; but from the frangible nature of the strata, it is not often easy to preserve them.
The following woodcut is from a beautiful specimen, from Chautauque county, where the
undulations of the ripple are perfectly preserved: -
* These separated laminae form large troughs, bowls, etc., which are frequently used in this part of the country as substi-
tutes for more perishable articles of the kind. At a farm-house, I have seen them used for wash-hand basins; and in other
places, I have seen the swine and barn-yard fowls feeding from similar forms. -
[GEoL. 4th DIST.] 33
:
:
258 GEOLOGY OF THE FOURTH DISTRICT,
:
114.
-
tº Hº
* tºurish
ſ * * º ſº
3. Žº º - - --- º-
ºft %|}}}#}/º/Wº%; |
§Z%% %%%);
º!4& %#%º:.”
This structure has been before explained as giving evidence of shallow water, and the
evidences exist in all the strata of the district which are composed of sand, or sand and clay
intermixed, from the Medina sandstone upwards. In the purely argillaceous and calcareous
strata, these markings are not seen.
In many places the rippled sandstones alternate with shale, presenting a very interesting
appearance. The edges of the sandstone are undulating, while those of the shale are horizon-
tal, and this is repeated several times in succession. The following section, from the banks
of the creek above Lodi in Cattaraugus county, illustrates this structure :
-------
Section of vertical cliff on Cattaraugus creek.
1, 3, 5. Horizontally stratified shale.
2, 4, 6. Undulating, arenaceous strata.
Localities.—There is scarcely a ravine, or bank of a river or stream in the southern range
of counties; where the rocks of this group are not exposed; therefore localities for examination
º
g-
.
f
tº º &
42 * . . ... • *
* * º, € er º
CHEMUNG GROUP. 259
are almost innumerable. There are a few points, however, where observations can be much
better made than at others, and where the different characters of the rocks and their contained
fossils can be more readily examined. - • r
Along the eastern side of the district, the Inclined plane of the Railroad at Ithaca, and the
Cascadilla and Fall creeks are the best localities for the lower part of the group. Farther
south, the banks of Cayuta creek, and the lateral ravines joining the same, offer good expo-
sures of the middle and higher parts of the group, with numerous fossils not seen at the more
northern localities. -
At the Chemung Narrows (see sketch at the head of the group), in the town of Chemung,
there is a very good exposure at a cliff upon the river bank, and the artificial excavation for a
road has much increased the value of this locality. Some of the quarries near Elmira are of
interest, but the exposures extend only to a few feet in depth. The hills in the vicinity of
Bath offer many interesting localities, and some fossils not elsewhere seen. At Painted-post,
along the excavation of the Blossburgh railroad, the strata are well exposed, and contain nu-
merous fossils. This is one of the most interesting localities in that part of the State, and
presents some features of the strata not so well exposed elsewhere. -
On the Genesee river, and in the banks of its tributary streams, there are several points of
great interest. The most northerly of these is Caneadea creek, where there is a great ex-
posure of green shale, with sandstones towards its termination. At Rockville on Black creek,
there is an exposure of green shale, becoming olive on exposure, which contains an abundance
of organic remains, and among these are several which have not been seen at any other lo-
cality. In the creek at Hull's mills near Angelica, there is a good exposure of shale and
sandstones with some fossils. At Hobbieville and Phillipsburgh, a few miles farther south,
we find an association of strata very similar to those of Rockville, and many of the same
fossils, together with numerous other species. This neighborhood is one of the most prolific
localities of fossils in the group, Farther south, at Wandemark's Creek, some of the higher
strata, loaded with a large Delthyris, are well exposed, and fine specimens can be obtained.
At Wellsville, a few miles south of the latter point, the rocks of this group terminate, and are
succeeded by SOIſle thin ferruginous strata of the Old Red Sandstone, and this again by grey
diagonally laminated sandstone and conglomerate. - -
In Cattaraugus county, there are good opportunities of examining the strata, at Bailey’s in
the town of Leon, two or three localities near Cadiz, and in the southern part of Great-valley.
The ravines on the south side of the Allegany expose the strata in numerous places, but there
are few points where fossils can be obtained. -
In Chautauque county, the deep ravine of Chautauque creek affords the best opportunity of
investigating the rocks of this group, which there contain numerous fossils. The outlet of
Chautauque lake at Dexterville also affords a good opportunity of examining the strata, which
in some parts are loaded with fossils. - -
The localities enumerated are sufficient for a thorough investigation of the group; those
upon the Genesee alone afford a very good exposure for a single line of section, but, as before
remarked, there are many variations of character in an east and west direction, which present
-- 33%
260 GEOLOGY OF THE FOURTH DISTRICT.
new and interesting features. The differences in the character, both of strata and of fossils,
on which subdivisions may be founded, will appear after an examination of these localities.
Thickness. – This group, in the eastern part of the district, can scarcely be less than 1500
feet thick. This thickness is estimated from the dip over a distance of thirty or forty miles,
and the height of the hills towards the southern boundary of the State, which rise to eight
hundred feet above the valleys. - - - - -
The summit of the Portage group, on the Genesee river, is less than 1200 feet above tide
water, and the lowest passes in the hills south of this, occupied by the Chemung group, are
from 1500 to 2000 feet above tide water. The highest hills toward the south part of the
State are scarcely less than 2500 feet above tide water, showing a difference of elevation
between the two groups of 1300 feet. Allowing for undulations, which render the dip irregu-
lar, the whole thickness is above 1500 feet. At the western limit of the State the group has
evidently thinned to a considerable degree, though no good opportunities of measuring were
presented. When examined beyond the limits of the State, the evidence of its diminution
becomes more apparent; and when we go as far as Indiana, the whole of this group and the
Portage is embraced in a thickness of less than 400 feet. Still farther west, it is very pro-
bable that they have disappeared altogether.
Mineral contents of the group. — There is little of interest throughout the whole extent of
this group. Some of the septaria present the same minerals as those in groups below. Iron
pyrites often takes the place of fossils, and carbonate of iron is very commonly found replacing
the stems of crinoidea and some other fossils. This mineral becomes more abundant in the
upper part of the group, and is rarely seen in the lower part. The decomposition of the rocks
gives rise to the sulphates of iron and alumina, showing the presence of iron pyrites very
universally diffused. The strata are often stained by the oxide of manganese, and the pro-
duction of wadd in many places proves its occurrence in the strata in considerable proportion.
Springs. –The same remarks apply to that portion of country occupied by this group of
rocks as the last. When covered by forests, the surface is well watered by perennial springs
and streams in great numbers. As the improvements progress, the wood is gradually cut from
the higher grounds and the broad sloping hill-sides; the surface being thus laid open to the
direct rays of the sun, many of the springs fail, and the small streams are dried up. The
present system of clearing the country, and the wanton destruction of the forests, will even-
tually produce serious evils, in the want of water; and the inhabitants should remember, that
unless they obey the laws of nature in this respect, their sins will be visited upon their chil-
dren, and they will be driven out, and a stranger shall possess the land. This subject will be
farther noticed under the chapter on agriculture. --- -
Agricultural characters. — The soil resulting from the decomposition of the rocks of this
group is a compact clayey loam, which, with the great abundance of angular fragments of the
rock, gives it the character which is termed “flat gravel.” The soil of the valleys, particu-
CHEMUNG GROUP. - 261
larly of the larger and deeper ones, consists of a large admixture of northern materials, among
which may be recognized the pebbles of the different limestones and of the Medina sandstone.
Sometimes pebbles of the harder strata of the Hudson-river group occur with these, and it is
probable also that some of the limestone pebbles may be of the lower limestones north of Lake
Ontario and of the Mohawk valley, although they are not distinguishable by their fossils, being
usually worn very small. -
These circumstances often cause a contrast in the productions of the neighborhood; the
valleys, from the calcareous nature of the soil, being good wheat lands, while that of the hills.
beyond the influence of northern drift is unfit for growing wheat after the first few years from
its clearing, unless properly manured. This soil, from its compact nature, is better adapted
to grazing than to grain-growing, and this adaptation is beginning to be well understood.
Organic Remains of the Chemung Group.
The rocks of this group abound in fossils, presenting a great variety of forms of the same
genera. In the Fourth District, few forms known in the Hamilton group extend into the
Chemung. Species of the Brachiopoda are almost equally numerous with the Hamilton
group, while Aviculae are much more abundant both in species and individuals. The species.
and individuals of Nucula and Cypricardia, and some others, are about equally numerous in
both groups. Trilobites are rare, and there are but few species of coralline fossils.
The fossils are often very unequally distributed through the strata; localities being found
where few or almost no fossils can be obtained, and again the strata are completely charged
with them. Different localities also often present a great abundance of certain forms which
are rare in others. - - - º
The green sandy shales of Rockville and Phillipsburgh contain a great abundance of fossils,
mostly of Avicula, Lima, Cypricardia and Inoceramus, while Delthyris and Atrypa are
much less common. Again, the dark sandstones and sandy shales of Painted-post, Jasper,
Troupsburgh and Dexterville, contain myriads of the little Orthis unguiculus, and large num-
bers of Delthyris, Atrypa, and more rarely Avicula. At Chemung narrows, several species
of Avicula, with large numbers of Atrypa and Strophomena, are found, with very few of the
fossils of the localities before noticed. Scarcely a locality abounding in fossils can be exa-
mined, but some new form will be discovered. In this respect this group offers a contrast
with the Hamilton, which, where well developed, will yield nearly all the known fossils in a
single line of section. This remark applies to the Fourth District, though changes are mani-
fested farther east. - .*
In the following woodcuts, the fossils are grouped principally according to the generic re-
lations, and they embrace the greater number of forms which have been seen in the district."
—ºme
* A large number of these will not appear in this place, but may be found in the forthcoming volume on the Palaeontology
of the State.
262 GEOLOGY OF THE FOURTH DISTRICT,
Some that could not be satisfactorily determined, and some others which have been figured in
the Report of the Third District, are not here presented. -
As just before stated, the remains of Crustacea are rare in this group, which in this respect
contrasts with the Hamilton, where, although there are few species, still they are abundantly
distributed. The head of Calymene Bufo, and the tail of Dipleura Dekayi, have both been
seen not far from Ithaca. - f .."
The following illustration is the only perfect trilobite found in this group in the Fourth
District : - -
Calymene nupera, n.s.-General form elongated,
sides parallel; head three-lobed, middle lobe largest,
and much extended anteriorly; articulations of the
abdomen eleven, of the tail? Eyes like those of C.
Bufo, but less prominent.
This fossil resembles the C. laevis of PHILLIPs,
Palaeozoic Fossils, pl. 55, fig. 250. -
Locality—Chemung creek.
N
§§
§
| Wºº
\
§
W §
ū §
}º
\\
§
sº
Among the Aviculae, the first two figures are typical of that part of the group about Che-
mung Narrows and several places in that county, and of the strata holding the same position
in other places. The two next figures are of species marking the brownish sandstones at
Painted-post, Jasper, and other localities holding the same position in the group.
117.
ºº:
#ſº
*
gºń º º; ...
ſº §: É
- º 32. Ží º
º 3: 3%- - 77.8
§ ºº::
*
s
sº
(ſ %& º º (
%| ſ º \\ ºl
# *% º º
|\º
§§§
§º
jº
1 and 2. Avicula pecteniformis. 3. Avicula longispina. 4. Avicula spinigera,
CHEMUNG GROUP. 263
1. Avicula pecteniformis, n. s.-Plano-convex; upper valve flat, surface (except the wings)
plain or with fine concentric striae; posterior wing with strong elevated radiating ribs; an-
terior wing acute, with a fold; lower valve slightly convex, surface and posterior wing marked
by strong radii or ribs of unequal size, which become obsolete or undulating toward the margin;
anterior wing with a single strong fold, and finer radii; posterior wing large, and extending
into an obtuse angle beyond the margin of the shell. - r-
The flat plain upper valve, and the unequal ribs which become obsolete toward the margin
of the lower valve, are distinguishing characters of this shell.
Localities—Chemung narrows; Cayuta creek.
3. Avicula longispina, n. s.-Obliquely subovate or elliptical, convex; surface marked
by concentric lines; beak prominent, extending above the hinge line ; anterior margin scarcely
produced into a wing, but slightly extended in a curve beyond a deep fold; posterior wing
very small, and suddenly extended into a long spine. - -
From the convexity of the shell, the wing and spine are usually covered, which may lead
to mistaking the fossil. It is not uncommon. -
Localities—Painted-post; Jasper; Cassadaga lake.
4. Avicula spinigera (CoNRAD, Jour. Acad. Nat. Sci., Vol. 8, p. 237, pl. 12, fig. 3).-
Obliquely subovate, with concentric lines and wrinkles; anterior wing short, obtuse ; posterior
wing small, suddenly produced into a long slender spine. - -
The spine is often broken off in removing the rock from around the shell, but some portion
of it can always be seen. In this species the spine is less parallel to the direction of the
shell, which is also smaller than No. 3; both often occurring together. -->
Localities—Painted-post; Jasper; Chemung.
1 18.
i. § §: º
º §§§
ºr SSS
WNº.
l, a and b. Avicula Damnoniensis. 2. Avicula acanthoptera.
1, a and b. Avicula Damnoniensis. (SoweRBy in Geol. Trans., New series, vol. 5, pl. 53,
fig. 22. PHILLIPs, Palaeozoic Fossils, pl. 23, figs. 90, 91, 92.) — Fig. 1 is the usual form;
a, a shorter variety; and b, a specimen compressed so that the wing is scarcely perceptible.
In these specimens, which are from the soft green shale of Steuben county, the longitudinal
striations are not visible ; though in specimens from other localities, they are distinct.
264 GEOLOGY OF THE FOURTH DISTRICT.
2. Avicula acanthoptera, n. S. — Obliquely ovate, with a small acute anterior wing ; the
posterior wing ending in an acute spine, which extends as far as a line parallel with the pos-
terior margin of the shell. Locality, Phillipsburgh. -
The following forms are found in the green and olive shales and shaly sandstones of Rock-
ville and Phillipsburgh on the Genesee, and they are the prevailing fossils. They are all
entirely distinct in form, and in the style of marking upon the surface.
119,
ſº
º
º
§º
1. Pterinea 7 suborbicularis. 4. Pecten cancellatus. 7. Pecten? striatus. 10. Lima glaber.
2. Pecten duplicatus, 5. Avicula? signata. 8. Pecten ? crenulatus. 11. Lima obsoleta.
3. Lima rugaestriata. 6. Pecten ? convexus. 9. Pecten ? dolabriformis. - -
1. Pterinea 2 suborbicularis, n. S. – Suborbicular, or broadly semi-elliptical; surface
marked by numerous, somewhat undulating ribs, which alternate with smaller ones toward the
margin; ribs crossed by concentric wrinkles, producing a rugose surface; wings scarcely
distinct; hinge line angulated at the extremities. - -
Locality—Hobbieville, Allegany county.
2. Pecten duplicatus, n.s.-Ovate-orbicular, equilateral, convex above; ears small, nearly
equal; surface marked by numerous radiating ribs, which are plain above, and equally can-
cellated by concentric lines, but becoming uniformly duplicate and rugose toward the base.
This fossil is readily distinguished by its great breadth and the duplicate rugose striae. It
bears some resemblance to P. plicata, Sowerby.
Locality—Phillipsburgh, Allegany county.
3. Lima rugaestriata, n. S. – Oblong, obliquely ovate, moderately convex; ears small, not
very distinct from the shell; surface with strong radiating striae, which augment toward the
base, and are crossed by elevated undulating lamellae, giving the surface a rugose appearance,
which is visible in the enlarged portion.
Localities—Rockville; Hobbieville, Allegany county.
CHEMUNG GROUP. - 265
4. Pecten cancellatus, m. s.- Obliquely ovate; ears small, distinct, posterior one rather
strongly plicated; (left valve) surface evenly cancellated by fine radiating and concentric
lines. - -
In form this shell resembles the last, but the striae are more even, and never rugose; the
form of the posterior wing is likewise different. - - -
Locality—Phillipsburgh, Allegany county.
5. Avicula? signata, n. S.–Obliquely sub-ovate; ears small, distinct, posterior one acute; .
surface marked by sharp concentric lines or lamellae, which give the shell a peculiar aspect.
Locality—Rockville, Allegany county. - -
6. Pecten? converus, n.s.—Orbicular, very convex; beak much elevated above the hinge
line; surface marked by radiating striae, which, are crossed by concentric undulating lines,
giving the shell a very pretty appearance. . .
This fossil is readily distinguished by its great convexity and orbicular form.
Locality—Rockville, Allegany county. -. -
7. Pecten striatus, n. s. – Erect, ovate; ears small, nearly equal; shell moderately COIl-
vex, surface finely and evenly covered with radiating striae. . . . .
This differs from all the others in the fine, even, radiating striae. -
Locality—Painted-post, Steuben county, in brownish sandstone.
8. Pecten? crenulatus, n. s. --Obliquely sub-ovate; posterior wing extending down the
side of the shell more than half way to the base; anterior wing short; hinge line crenulated;
surface of the shell faintly marked by obsolete, radiating and concentric lines.
Locality—Rockville, Allegany county. - - -
9. Pecten? dolabriformis.-Obliquely suborbicular, moderately convex; ears small, pos-
terior one sharply angulated; beak a little elevated above the hinge line; surface marked by
fine radiating and concentric striae. - i
This shell somewhat resembles No. 6, but is much less convex, more oblique, and the pro-
portion of the ears different.
Locality—Phillipsburgh, Allegany county. .
10. Lima glaber, n. S.–Erect, oblong-ovate; hinge line very short; ears small; shell
very glabrous, with a few concentric, scarcely visible undulations. -
The distinguishing character of this shell is its elongated form, its narrowness just below
the hinge line, and the very glabrous surface. - -
Locality—Phillipsburgh, Allegany county.
11. Lima? obsoleta. —Somewhat obliquely ovate; slightly convex; surface faintly marked
by concentric lines, which are stronger upon the ears; hinge line crenulated. This fossil is
referred, with doubt, to the genus Lima, the hinge being crenulated. - -
Locality—Phillipsburgh, Allegany county.
[GEol. 4th DIST..] 34
266 GEOLOGY OF THE FOURTH DISTRICT.
Among the Brachiopoda, the following have been selected as most characteristic of the
group, though there are other species, perhaps, equally numerous. . . .
120.
1. Strophomena nervosa. 3. Strophomena arctostriata. 5 a, b, c, Strophomena interstrialis.
2. Strophomena bifurcata. 4. Strophomena pectinacea.
1. Strophomena nervosa, n.s.-Semicircular, with the hinge line greatly extended, forming
a spine-like prolongation; surface marked by undulating, nerve-like striae, which augment in
number toward the margin, and between which are finer striae. * ,
1 a. An enlarged portion of the shell. The shell resembles the nerved wings of some
insects, which with the greatly extended hinge line is sufficient to distinguish it.
Localities—Bath; Campbelltown. " .
2. Strophomena bifurcata, n. S. – Broadly semi-elliptical; hinge line extended beyond the
width of the shell, and angulated at the extremities; surface marked by about 34 to 36 ribs
at the hinge, which uniformly and regularly bifurcate once or twice before reaching the margin.
This is a widely distributed fossil of the Chemung, extending over 150 miles in an east and
west direction. - - -
Localities—Napoli, Cattaraugus county; Chemung.
3. Strophomena arctostriata, n. s.—Broadly semi-elliptical or semicircular; lower valve
very convex, slightly impressed in front; hinge line scarcely extending beyond the width of
the shell; surface covered with numerous, crowded, unequal striae. -
Localities—Hobbieville; Chemung.
4. Strophomena pectinacea, n.s.-Semi-oval; lower valve very convex; hinge line shorter
than the greatest width of the shell; surface marked by from 24 to 28 prominent sharp striae,
with two or three intermediate ones which are less prominent.
This fossil somewhat resembles the next species, but the striae are more prominent and
fewer in number. It is a widely distributed fossil in this group. .
Localities—Hobbieville; Rockville; Cattaraugus county.
CHEMUNG GROUP. 267
5 a, b, c. Strophomena interstrialis (Orthis interstrialis and Leptana interstrialis, PHIL-
LIPs, Palaozoic Fossils, pages 61 and 216, pl. 25, fig. 103). — Semicircular; lower valve
convex, upper one flat or slightly concave; surface marked by sharp radiating striae, which
are sometimes continuous to the margin, and at others interrupted or divaricating; between
each pair of these striae are four or five others, much finer, and slightly undulating.
5, is the inner side of the flat valve from Chemung. -
5 a. A magnified portion of the shell. -
5 b. The two valves, somewhat compressed, from Ithaca. -
5 c. The convex valve, with the shell partially removed, from near Elmira. -
The S. inequistriata and S. mucronata (Jour. Acad. Nat. Sci., Vol. 8, p. 254 and 257,
pl. 14, figs. 2 & 10), appear to be identical with this shell of Mr. Phillips, and since his name
has precedence, it is retained. It is readily known from the character of its larger and finer
striae, in which it resembles the S. sericea and S. transversalis, from both of which it is quite
distinct. - - -
It is one of the most widely distributed fossils in the group, and has a somewhat different
aspect in the shales, sandstones and calcareous layers. -
121.
º
§|#| || W
㺠l º
: * ; * º
sº
º º \ º i
*º
º
º
§
º | º º
º
1 and 1 a. Orthis carinata. 2. Orthis impressa. 3 and 4. Orthis interlineata. 5. Orthis unguiculus.
1. Orthis carinata, n. s. – Semicircular; lower valve very convex, with a depression ex-
tending from beak to base ; surface covered with fine radiating striae ; upper valve flat, with
a sharp ridge along the centre, which is very prominent in the cast; cast of the subrostral
impression very prominent and acute at the beak, and not deeply indented below.
1, lower valve; 1 a, upper valve. -
This character of the cast of the upper valve is always sufficient to distinguish the shell,
and it is usually the most obvious character. .
Localities—Painted-post; Chemung; Jasper, in brown sandstone.
34*
268 GEOLOGY OF THE FOURTH DISTRICT.
2. Orthis impressa, n. s. – Circular; hinge line short; upper valve nearly flat, suddenly
depressed in front (as if the finger had been applied when the shell was flexible); surface
covered with fine equal striae, which are more strongly marked upon a narrow border on the
margin; cast of the muscular impression at the beak small, bilobate by a narrow sinus.
The form is perfectly represented in the figure, which is a cast. It is often associated with
the next species in the soft and green shales about Elmira and elsewhere. -
3 and 4. Orthis interlineata (SowerBy in Geol. Trans., 2d series, vol. 5, pl. 54, fig. 14.
PHILLIPs, Palabozoic Fossils, p. 63, pl. 26, f. 106.) *s Transversely elliptical, depressed;
hinge line much less than the width of the shell; upper valve flat, with a ridge along the
centre; lower valve moderately convex, with a shallow depression from beak to base; surface
radiated by numerous unequal or divaricating striae.
Fig. 3 is a cast of the upper valve, in which the inequality of the striae are less perceptible.
Fig. 4, lower valve, showing near the beak the spaces from which the subrostral plates
have been removed. . . . r -
The figures of Sowerby correspond better with our fossils than those of Mr. Phillips. The
casts, however, fig. 3 above, and 106 a of the latter, very closely resemble each other, and
there can be no doubt of the identity of the fossils. r
Localities—Cayuta creek; Chemung; Elmira.
5. Orthis unguiculus. (Atrypa unguiculus, SoweRBY in Geol. Trans, 2d series, vol. 5,
pl. 54, fig. 8. Spirifera unguiculus, PHILLIPs, Pal. Fossils, pl. 26, f. 119.)—Hemispherical,
varying in the proportions of length and breadth; beak large, inflated and incurved; lower
valve very convex, with a central impressed line extending a part or the whole distance from
beak to base; upper valve flat, or slightly convex on each side of a depressed line in the
centre. - .
This fossil usually appears as casts, frequently abundant, and covering surfaces many feet
in extent. - - . . .
5 a. Cast from Bald hill, near Ithaca. - -
b. Lower valve; broad variety. Dexterville, Chautauque county.
c. Upper valve. Painted-post, Steuben county. - -
d. Fragment of brownish sandstone, covered with casts of the shell. Jasper, Steuben
county. '; .
This fossil differs from the O. umbonata of the Hamilton group, which it considerably
resembles. - - -
CHEMUNG GROUP. 269
122.
i
#
#
|d
|
|
;
". |
ºf | |
ºf
|
|
º|
|
|
1. Delthyris mesastrialis. 2. Delthyris mesacostalis, 3. Delthyris disjuncta.
1. Delthyris mesastrialis, n. S.–Semicircular; hinge line extended into short, acute ears;
upper valve broadly emarginate in front; mesial fold very broad and deep, finely striated, and
well defined; surface marked by from fourteen to twenty rounded ribs on each side the
mesial fold; ribs prominently rounded and finely striated longitudinally. The ribs are some-
times crossed by a few elevated laminae of growth, as in fig. 1, the upper valve; while in 1 a,
the lower valve, they are not visible. - -
The beautifully striated mesial fold is alone sufficient to distinguish this shell from any other
in the group. Of two others with a striated mesial fold, one has flat and the other very sharp
ribs. - - ..)
Locality—Cayuta creek.
2. Delthyris mesacostalis, n. S. – Sub-rhomboidal; beak very much elevated above the
hinge line ; hinge extremities terminating in abruptly acute ears; lower valve very convex;
mesial sinus angular, deep, and with an obtusely angular rib along the centre; surface marked
by about fourteen obtusely angular ribs on each side the mesial fold.
The angular rib in the centre of the mesial fold, with the nearly equal length and breadth
of the shell, are the distinguishing characters.
Locality—Angelica, in grey sandstone.
3. Delthyris disjuncta? (PHILLIPs, Palaeozoic Fossils, pl. 29, fig. 128, f, g, h, and 129;
pl. 30, fig. 129.)—Semicircular, convex, broadly emarginate in front; hinge line extended
into short acute ears; mesial fold broad, not defined at the borders; surface marked by
twenty-five to thirty small plain ribs on each side the mesial fold; radii on the mesial fold
smaller, and bifurcating toward the margin, where there are often fifteen in number.
270 GEOLOGY OF THE FOURTH DISTRICT.
The principal differences between this description and that of Mr. Phillips is that the mesial
fold is not deep, and the ribs are not divaricating or duplicate toward the margin, except as
mentioned. - - -
Locality—Chemung, associated with Atrypa laticostata, in great numbers.
§ sº * § §§
|; i. A. º § º
§s
-
: º \
º
sººººººº
º \
º/ſº §º s W
§§
ſº
º -
ſ w
N
w
#|
- .."
§ ..”
º ,”
º
º
º
1. Delthyris cuspidata. 3. Delthyris mucronata 5 and 5 a., Delthyris acuminata,
2 and 2 a. Delthyris acanthota. 4 and 4 a. Delthyris inermis. -
1. Delthyris cuspidata, m. s. – Somewhat semicircular; hinge line extended into acute
ears; broadly emarginate in front; mesial fold broad, moderately deep, and undefined at the
borders; surface marked by many equal entire ribs (about 30 on each side the mesial fold),
those on the mesial fold smaller; ribs crossed by elevated lamellae toward the margin of the
shell. -
It is perhaps not improbable that this fossil may be referred to some variety of Spirifera
disjuncta. (Sowl:RBy, Geol. Trans., New series, vol. 5, pl. 54, figs. 12, 13; pl. 55, fig. 2.
PHILLIPs, Palaeozoic Fossils, pl. 29, fig. 128, f, g, h, and fig. 129; also pl. 30, fig. 129.)
Localities—Cayuta creek; Chemung; Vandemark's creek on the Genesee river. Often
occurring in immense numbers. * - - -
2. Delthyris acanthota, n. s. – Semicircular; hinge line greatly extended into long acute
ears; emarginate in front; mesial fold well defined, often oblique, expanded at the base, and
marked by divaricating striae; shell marked by about eighteen equal undivided ribs on each
side the mesial fold, and five or six smaller ones on each wing.
2, the upper, and 2 a, the lower valve.
CHEMUNG GROUP. 271
There is considerable resemblance between this shell and the last, and they may prove to
be varieties of one species, the hinge line more extended in the younger ones.
Localities—Ithaca: Cayuta creek; Chemung.
3. Delthyris mucronata? (See page 205, fig. 3.)—Transversely elongated; hinge line
extended into mucronate points; beak little elevated above the hinge line ; mesial sinus well
defined, with a small rib in the bottom; surface marked by about fourteen rounded, imbricated
ribs on each side the mesial fold. 3 a, an enlarged portion of the shell.
This fossil differs in no respect from the D. mucronata of the Hamilton group, except the
rib in the centre of the mesial sinus. It is referred to this species, till more specimens have
been examined. Locality, Troupsburgh, Steuben county. - .
4. Delthyris inermis, m. s.-Semicircular; beak of the lower valve much extended above
the hinge line; hinge line not extending beyond the shell; surface marked by about twenty-
five equal, simple ribs on each side the mesial fold; mesial sinus deep and well defined,
marked by about eight divaricating ribs, which are smaller than those on either side.
This fossil is very abundant in Chautauque county, forming layers of several inches thick
and many yards in extent. Localities, Chautauque creek; Twenty-mile creek.
5. Delthyris acuminata, n. S.–Transversely elongated; hinge line much extended into
long acuminate points; mesial fold simple, well defined; surface marked by sixteen simple
ribs, which are crossed by abruptly undulating elevated lamellae, usually much better seen in
the external casts of the shell. &
5 and 5 a. Internal casts of the upper and lower valves.
5 b. Enlarged portion of a cast of the external surface,
Localities—Ithaca: Chemung; Cayuta Creek,
124.
1. Atrypa dumosa. 2. Atrypa hystrix. 3. Atrypa tribulis. 4. Atrypa" tenuilineata,
272 GEOLOGY OF THE FOURTH DISTRICT.
1. Atrypa dumosa, n. S.–Semicircular, or somewhat transversely elliptical; beak of the
flatter valve scarcely prominent; surface marked by about 32 rounded radiating ribs; the
ribs are crossed by elevated, concentric, undulating, thread-like lines, and at more distant
intervals, elevated lamellae; the lamellae upon each rib are folded into a short round spine.
Fig. 1 and 1 a, are faithful representations of two specimens, the latter imperfect.
1 b. Cast of the interior of the flat valve, punctured throughout, except the subrostralim-
pression. • . . . .
This fossil is abundant, though the spines are usually removed, and the surface presents a
squamose appearance, which had induced me to refer it to A. squamosa of Sowerby.
Localities—Chemung; Cayuta creek; Elmira. -
2. Atrypa hystria, n. S.–Transversely subelliptical, often approaching to circular; beak
scarcely prominent; surface marked by about eight broad ribs, which are crossed by five or
six elevated lamellae; at the junction of these with each rib, proceeds a long slender spine.
This fossil is totally distinct from any form of Atrypa figured, and is one of the most
striking fossils in the rocks to the south of Bath, Steuben county. . .
3. Atrypa tribulis, n. S.–Hemispherical; upper valve very convex, with the lateral edges
pressed downwards; lower valve nearly flat, elevated in front, and reflexed at the sides;
beak rather prominent; surface marked by numerous divaricating radii, which are crossed by
few concentric lines of growth. - -
3, lower valve. 3 a, upper valve. 3 b, cast of the interior of the flat valve.
There is considerable resemblance between the cast of this fossil and that of A. dumosa
(1 b), but on closer comparison, they will be found to differ essentially. In this species, the
cast of the subrostral depression is longer and less strongly defined; the subrostral plates
are likewise compound, while they are simple in A. dumosa. This will be seen by the small,
projecting, tooth-like process, extending into the space on each side the beak, and which
shows a division of the plates, which were proportionally larger than in the other species.
Unlike as these fossils appear, it is often difficult to distinguish them under different
aspects, when imbedded in a different matrix, and in various stages of perfection. The casts
of these, as well as other species of the genus, will be found reliable. *
There is a very close resemblance between this fossil and the forms usually refered to A.
prisca, A. affinis, &c., and I was disposed to refer it to that species; but further examination
has induced me to consider it distinct, until an opportunity offers of examining the internal
structure of those analogous or identical species in the lower rocks.
Localities—Ithaca ; Chemung; Elmira.
* . \ .
4. Atrypa tenuilineata, n.s.-Nearly circular; beak small; surface marked by numerous
very fine radii. . -
It is possible that this fossil is an Orthis.
Locality—Cattaraugus county.
CHEMUNG GROUP.
273
and
5
it appears
like a species of Filicites; but from its uniform
or perhaps
but beyond
these two forms, the species are all limited
2
that I have thus
far been unable to satisfy myself of its proper
5
; and in one or two
localities, I have seen a specimen of the Tur-
it seems more like the
The little Millepora gra-
cilis is found from one extremity of the district
to the other.
In the Fourth District, there are few fossils
There is also a species of Rete-
Near Bath, and at Chemung,
there is a species of Cyathophyllum which has
At Ithaca, Hector and Enfield in Tompkins
county, the fossil of which the accompanying
- It occurs in single detached speci-
mens, or in tufts which appear to have centered
figure is an illustration, is found in considerable
The structure is so minute
size, the regular angle at which the leaves are
given off from the stipe, and the absence of
carbonaceous matter,
stipes, all apparently centering at one point at
relations, and it is left for further investigation.
The specimen figured presents parts of several
the base, and slightly diverging above.
belonging to the Polyparia, but some of these
forms are abundant.
in a single base or root. At first view,
more analogous to the Sertularia.
pora which is equally abundant;
tentaculated fingers of a crinoidean,
occur but rarely.
not been seen elsewhere
binolopsis.
numbers.
######
===~}
%2，5-=
ſ/~
}^：
%
`№， №）：
žé£№.）ſae%%：ſºſ|}，ź %%|||||ğ
：'''|ſae. ： |-ſae
|
，，….… ！
：Ø
ſ///////////////
|（~~~~ （№
\\
%
**º
35
[GEOI. 4th DIST.]
274 "'. GEOE,OGY OF THE FOURTH. DISTRICT,
It has before been mentioned that some fragments of land plants have been noticed in the
lower part of this group, and even as low as the Genesee slate. In the eastern part of the
State, as will be seen from the Report of the Third District, some similar fragments have
been found as low as the Hamilton group, but these have not been observed in W estern New-
York. As we approach toward the termination of the Chemung group, we find some forms
very analogous to those of the Coal formation, giving evidence of the approach to that period.
These may have drifted from dry land farther east, and in many instances have undoubtedly
done so; in others, from the perfect preservation of the fragments, it seems hardly possible
that they could have drifted far, except in a quiet sea. - --
Most of the specimens obtained have been fragments, however; and of the more solid
portions of the trunk, a few fragments of ferns have been found, and a single specimen in a
tolerably perfect condition, of which the opposite page exhibits an illustration. *
It appears referable to the genus Sphenopteris, but differs from any figure in Brongniart's
Végétauw Fossiles, which is the only work of reference within my reach. The name law.us
is suggested from the want of rigidity in the branches, which characterizes most of the species.
This unique specimen was obtained by Mr. E. Sexton, of Pine valley, Chemung county,
from his quarry in the vicinity; and through his liberality, it has been placed in the State
Collection. - - -
The quarry referred to presents a peculiarity in the arrangement of the strata, not else-
where noticed; the lower beds have a uniform northerly dip, while a thin bed of similar
materials resting upon these, dips in an opposite direction, as represented in the section below.
The position of this quarry is just below the more highly fossiliferous rocks of the Chemung
group, which occur in the same hill, , -
º->- -- E=E
C--~-->
Section of Sexton's quarry, Pine valley, Chemung county.
Fragments of fossil vegetables referable to the genus Sigillaria, occur somewhat rarely
in the higher rocks of the group. A fine specimen of this character was obtained by Mr.
Horsford in the vicinity of Black Creek; and another, of which the illustration is also on the
opposite page (fig. 2), was found in Wisner's quarry near Elmira,
Other specimens referable to the genus Calamites have been observed in the rocks of this
group, and some in which no definable structure exists.
CHEMUNG GROUP 275
127,
\
\
s
|
\-
}
W.
º
º
ſ
º
- ºš
KºšW.A
- &\º
§ * s §
§ N Wºº
sº §
§º
ŞN
§
º
\
\
N
ºº:
ſ
N
º
§
º
N
§§
&\
\ W º
WN º N W
§§
|
ºº
§
\
º
/
\
ſ
&
W
§º
§º
tº. º \ \\ \ W
\ º º
§Wº º \
§§
º
º
|
N
ºsº
º-E.
º
§-
|
º:º
Nº; §* ,º
i-:ººſ
º§º|
§§wW
ºº~iN
§--ºº
º -ſº
§º
º:§
W
2
º|
§
Nº
|
W
§
|
f
|
º
a
|
|
}
\
|
|
§
|
h\
W
|
\
W
tº
|
\
W
|
|
§
º
ºº
s
º º
º º }|\º
º º ſº
º º º
% % º §
% º
-- * W \
$º ſ }\\\\\ |||}}} º º § W W \\
A
§§ § \ \\
|ſ
|
\
N
Nº
|
|
|
|
|
|
|
|
|
|ſ
%
º(ſ
ºº
ſ
\
W
|
|
\
|
W
bill
%
*
%
à
ſ
|
ºh\
§
%*-3*}
ga* :|
g#\
sº:§§-
§º
&:B
ſ§*º-
W g W
#
%
wº
º
|
º
-º-º-º:
|º%%}
ſ
ſ | W º y
| º s
º
|
ſ
|
º
ſ
ſ
ſ
& º
N º tº
º W. sº
fl
º
|
ſ
;|
º
||
|
ſ
}\;\|\!\!\!\||
º º |
§
- º
º § º § º
}:
º
§ |
º | º §
ŠN
|
|º
|-|
| º \ º
ſ
sº º §º #º
tº 3% ºf
j
º
º
g
&
ſ
º2źi.:!
%§:
|
|
º
ºº |
º %
§ -
|
|
|||}} % ſ||
% º %
º
º #
\
|
º
|
ſ
|
º
|
|
º
;
f
|
|
º \
|
ſº
\
ill º º & º
ºſº º
º º
º º º
# | ſ
ji,
%
J.
ſ
º
#/.
W
|
\
ºsº º
\\ º ſº *\\ |
| |\\ eſ
§ l
\
º
º
\
\
§
|
*
º
º: º %
@%|||}
ſº
%
º % ſº
; % fº § %Ž §
§ % %º §º
%
1. Sphenopteris laxus. a 2. Sigillaria Chemungensis—one-half the natural size.
276 GEOLOGY OF THE FOURTH DISTRICT.
Localities of Superposition.
There are few localities, where the junction of this group with the one next above is obvious.
Throughout the greater part of the district, the higher rocks have been removed by denudation.
In a few points, it is succeeded by a thin band of the Old Red sandstone, which is a highly
ferruginous stratum, and contains few fossils. In other places, the conglomerate of the Coal
formation rests directly upon the Chemung group.
The section, page 253, shows the order among the rocks of the Chemung and the successive
formations along the Genesee river. The same is seen in the section of Allegany county,
Plate 11. In Plate 10, the section across Steuben county shows the Old Red succeeding the
Chemung. In Plates 11 and 12, the sections of Cattaraugus and Chautauque counties show
the conglomerate resting upon the Chemung group. This occurs from the thinning out of the
Old Red sandstone, as will be seen under the description of that rock. -
The series even where the Old Red intervenes is nevertheless incomplete ; and the perfect
order of succession from this point upwards cannot be established in New-York, from the
absence of the Carboniferous limestone. . -
With the rocks of the Chemung group, terminate all those included in the New-York
. System. The reasons for uniting all the rocks and groups below the Old Red sandstone in
one system, and for considering the latter as distinct, have already been stated briefly. The
termination upwards of the Chemung group has been shown in the sections given, and the
character of the strata composing it fully described. It will be seen, that in the eastern part
of the State, many of the fossils of the Hamilton group extend into the Chemung, and at the
same time the lithological character is nearly the same in both. Farther to the west and
southwest, the lithological character of the two groups is quite different, and at the same time
we find few of the fossils of the lower group extending into the higher. Even where there
is the greatest distinction in lithological and fossil characters, the two can only be separated as
parts of a great system, being the productions of continually operating causes from beginning
to end. The products differ in character, and the fossils are of different species, but they are
of the same prevailing genera. - - f
Where the best opportunities for examination exist, the change from the Chemung to the
Old Red sandstone is abrupt in character. The greenish and olive shales and sandstones
charged with Strophomena, Delthyris and Atrypa, are succeeded by a red sandstone, con-
taining none of the organic remains of the lower rocks. The change in lithological character
is accompanied by a change in the fossils, even more decided. Few shells are known, but
the rock every where contains the remains of fishes, which are often preserved in a very
perfect manner. - -
It is quite evident from lithological character alone, that these two deposits are not syn-
chronous; the materials differ in character, and the extent of the higher rock is very limited.
The Old Red sandstone is scarcely known west of the Genesee river, where the Chemung is
CHEMUNG GROUP. - 277
in greatest force; and from this early thinning in a westerly direction, as well as from other
facts, it is evident that it had not the same origin as the rock below.
In examining rocks westward, the place of this never presents any remaining matter that
indicates its former existence, or any marks by which we can infer that it has been previously
swept off. In many places the conglomerate rests upon the Chemung group, without the
intervention of any other rock. *. S -
The rocks of the New-York system, although many of them diminish westward, are most
or nearly all of them represented as far as the Mississippi river. The change, for the most
part, is well marked in all cases between them and the higher rocks, and they as evidently
constitute one great system over all this extent of country.
It may not be out of place here to remark, that the rocks of the Chemung group are
regarded by some geologists as forming a part of the Old Red sandstone, and that the
“Devonian system” of Mr Phillips includes both these rocks and the red sandstone which
succeeds them. I have already remarked, that in the eastern part of New-York, there are
many fossils typical of lower rocks which extend upwards into the Chemung group; and
should the latter be united to the Old Red, it offers too intimate an association of strata, and
of organic remains, to allow of any separation beyond that of simple groups; whereas by
leaving the Chemung united to the rocks below, we have a very marked change in the
productions of the succeeding formation. --
278 GEOLOGY OF THE FOURTH DISTRICT.
CHAPTER v1.
\-
OLD RED SANDSTONE.
Catskill group ; Montrose and Oneonta sandstone of the Reports.
- (No. 11 of the Pennsylvania survey.)
The rocks now recognized as belonging to the Old Red Sandstone, where fully developed,
consist of various strata of sandstone, shale and shaly sandstone, conglomerates and impure
limestones. The prevailing color of the arenaceous portion is brick-red, though often lighter,
and sometimes of a deeper color from a larger proportion of iron; while the coarser parts are
often grey, and the shales are green. Beds of green shaly sandstone are interstratified with
the red friable sandstone, and these are succeeded by a compact kind of conglomerate rock.
The strata rest conformably upon the grey, olive and greenish shales and sandstones of the
Chemung group, and pass beneath the conglomerate of the Coal measures. (See Section,
Plate 7, and woodcut below.) -
In the Fourth District, this formation is of no great thickness or extent; but in passing
eastward, we find it expanding and augmenting in thickness, till finally it rises in the high and
prominent peaks of the Catskill mountains, the highest of which has an elevation of more than
three thousand feet above the level of the sea. From the diminution of the lower groups, the
base of this formation approaches the base of the mountains, giving a great part of their
elevation for its thickness. - - -
Along the Genesee river, and in some of the higher hills south of the Canisteo in Steuben
county, it consists of a thin mass of calcareous sandstone, highly charged with iron, and con-
taining remains of fishes. By tracing it southward, it is found to expand, and presents many
of the features of the same farther east. It rises from beneath the Coal measures of Penn-
sylvania, extending northward, and resting upon the rocks of the Chemung group, as in
England it does upon the Ludlow formation, the equivalent of the latter.”
1. Chemung group. 2. Old Red sandstone. 3. Conglomerate, and diagonally laminated sandstone. 4. Coal measures of
Pennsylvania.
128.
* Compare the woodcuts, No. 128, and Plate 7, with the sections, Plates 31, 33, &c. of Silurian Researches.
*
ÖLD RED SANDSTONE. 279
The whole series has not yet been sufficiently investigated, to know if it admits of the same
subdivisions here as in England; yet it is very true, that to a certain extent, it possesses the
same lithological characters, and contains some at least of the same organic remains.
The existence of this rock, although so well known in England and some other parts of
Europe, was for a long time considered enigmatical in this country; and it is only since the
commencement of this survey, that it has been satisfactorily identified by its fossils.
In 1824, Prof. Eaton first suggested the existence of the Old Red sandstone on the Catskill
mountains,” though he appears to have overlooked this fact in his subsequent arrangements.
Some years afterwards, R. C. Taylor, Esq., in a report upon the Coal region about Bloss-
burgh, Pa., mentions the Old Red sandstone as existing there, and between that point and the
State line on the north. There was no other notice of its existence in this part of the country,
till the publication of the Geological Reports for 1840, when it was fully identified by its fossils.
To the west of the Genesee, I have only detected this rock in loose masses upon the
surface, though it is possible that it may occur at some of the elevated points, which, from
being entirely covered by forests, have escaped observation. Farther west, however, where
good opportunities for examination exist, it is not found; and it thus becomes evident, that in
this direction the rock disappears not far from the Genesee, in Allegany county. From this
fact it will be perceived, that there is a very rapid diminution in thickness from the Catskill
mountains to the point of its disappearance. This shows a condition of the primeval ocean
greatly different from its state during the deposition of the preceding groups, where a series,
with a thickness less than this one in its greatest development, extends nearly or quite as far
as the Mississippi, more than one thousand miles beyond the termination of the Old Red sand-
stone. This change in condition was evidently, in part, a diminution in the transporting power
of the oceanic currents, which had previously carried forward similar materials over the broad
extent before described. Other changes may have supervened, but we can scarcely conceive
of any other which would produce similar phenomena. - ~,
The materials forming the Old Red Sandstone are, to a great extent, as easily transported
as those of the rocks below; still their extent is limited in New-York, and westward as far -
as Ohio this rock is not represented at all. Still farther west the rocks of the Chemung
group are succeeded by sandstones and thin beds of limestone, wholly unlike the red and
green sandstones and sandy shales of New-York; and they contain, at the same time, a
different assemblage of organic remains. Other changes, too, have supervened at the west,
of which we have no evidence in New-York; and the most striking is the occurrence of an
important mass of limestone below the conglomerate, which is the great supporting rock of
the Carboniferous system.
In order to institute a comparison between the rocks of this period in New-York and those
at the west, the following woodcut, illustrating the relative position of rocks in Indiana, will
serve to give the reader all necessary data. - **
* Canal Rocks, p. 92.
280 GEOLOGY OF THE FOURTH DISTRICT.
1. Chemung group. 2. Grey sandstone, with beds of oolitic limestone. 3. Grey limestone, oolitic above. 4. Diagonally
laminated sandstone and conglomerate. 5. Coal measures. . -
In the Fourth District, the thinning margin of the Old Red Sandstone, from the large pro-
portion of ferruginous matter it contains, has usually more the appearance of an iron ore than
a sandstone. It appears to be a compound of sand, clay, and calcareous matter, with a large
proportion of the hydrate of iron, and contains, in abundance, small fragments of bones and
scales of fishes. These are generally too small and too much worn to be recognized, except
in the general similarity with better characterized specimens of scales and bones of Holop-
tychus from other localities. In some places the whole mass is an iron ore of tolerable
quality, containing probably 20 or 30 per cent of that metal. In such cases, however, it is
very thin, and I have been unable to find any rock above it in connection. -
This rock is much better developed in the First and Third Districts; and it is to be hoped
that some one with powers of investigation and description, like Mr. Miller of Glasgow, will
one day give us a work upon the Old Red Sandstone of the Catskill mountains, similar to his
on the same rock in Scotland.” -
\
Localities. – The principal localities where this rock can be seen in the district, are near
Wellsville on the Genesee; and at another point near Spring mills, in the southeastern part
of Allegany county. It likewise appears in several places in Steuben county, on the tops of
the hills between the Canisteo and the south line of the county. -
The mass is too limited in extent to produce any important influences upon the surface OT
soil, though it tinges the latter of a deep red, like the red shale of the Onondaga salt group.
Organic Remains of the Old Red Sandstone.
- In passing from the rocks of the Chemung group to the Old Red sandstone, we find a marked
change in the organic contents. Immediately below the latter we have green shales and shaly
sandstones charged with shells of Delthyris, Strophomena and Atrypa; while after leaving this
** ---
* Few works have ever appeared on the subject of geology, of greater interest than the book entitled “The Old Red
Sandstone, or New Walks in an Old Field,” by Hugh Miller. The clear and fascinating style of the author has here rendered
highly interesting, what in most other hands would have consisted so much of dry detail as to have been forbidding to many
readers. This work, and other writings of the same author, show what can be accomplished by a man who began life as a
quarryman, and who, having toiled through all the privations and discouragements of that kind of life, now stands among
geologists in such a position that the Rev. Dr. Buckland offers to give his right hand to possess the same felicity of descrip-
tion as Mr. Miller. - - - -
OLD RED SANDSTONE. 281
rock, we find nothing of that character. The shells which occur in the Old Red, so far as known,
are quite distinct from those of the Chemung. The most characteristic fossils are the bones
and scales of fishes. These meet the eye in all localities, from their strong contrast with the
ground in which they are imbedded, being usually nearly white or bluish in the brownish-red
rock. These scales and bones are often in minute fragments, and so permeated by iron as to
offer no contrast in color; but in other places they are perfect, and from an inch to one and a
aalf inches in diameter, appearing like patches of extraneous matter. -
By far the most common of these are the scales of Holoptychus nobilissimus, a fossil well
known in the same rock in England and Scotland. -
Scales of Holoptychus nobilissimus and Sauripteris Taylori.
The enamel of the scale (fig. 2) is marked by large undulating furrows and ridges, which
become obsolete towards that side covered by the scale next in front. This character alone
seems sufficient to indicate the fossil. The enamel is often removed from weathering, and
casts of its outer surface are preserved in the rock.
Many fragments of bones and some of teeth have been found in the same situation with
these scales (fig. 4 of woodcut 130 is one of these). Some of the teeth bear a very close
analogy to the figures of the teeth of Megalichthys. The fragments of bones often resemble
those of the buckler of Cephalaspis. : -
The jawbone with teeth of the following figure were found in the same association. The
whole length of the jaw was about seven inches. From the prevalence of scales of Holop-
tychus, I had supposed it to belong to that fish, but farther examination has led me to doubt
the correctness of this opinion. * - -
[GEOL. 4th DIST.] 36
282 - GEOLOGY OF THE FOURTH DISTRICT,
131.
gºzº.º. 3. º % ºft. 3 ºf A &
zºº/ſºliº
º, sº
E :FE
======= -
##############:s:=º
Eºs:#5:###:##$
Sº º -
š - ſº
º
š
====== 3::::::::::::::::=#####s===---. Tºš - =#sº
º:########## :=º := :=#sº ºf: v. 3. š;
##############.º.º.º.º.º.º.º.º. §§ §
É #º §/. $; % % % º § * % N %\\ º #. M º \ º \ ſº } -------- - ===s* º Bºº. §§ j -
tºº/\% }% % \º lºft % § º ;sº;|
2. \\?\\\\\\%lº % !/. % %;= j;|
jº \\ \ \% % ſºft % | % % % º % #% Ż 2; ſº
%iº
% % Ž % % % % % ºffº/jft); /§% %% º % *% % % % # , ºft ſº
§§ ########### ;#ffff:#ff §
WWººDºº gºv
Besides these, I obtained in a lower situation in the rock a fin and a large number of scales.
The fin presents a structure differing from any fossil fish of the Old Red sandstone which I
have seen described, and evidently partakes of the nature of the fish and the Saurian. From
this character of the fin, I have proposed the name Sauripteris.”
GENUs SAURIPTERIs.
Provisional characters—Pectoral fin composed of the rudiments of a humerus, the radius
and ulna, and phalanges; from the latter of which proceed bony rays. Enamel of the scale
punctured, as if for the insertion of small bristly points. The surface is slightly corrugated,
bearing the character of shagreen. -
Sauripteris Taylori (plate 3, figures 1, 2, 3, and fig. 1 of woodcut). — This fossil consists
of the clavicle with the rudimentary bones just mentioned, from which proceed bony rays.
Some thick heavy bones, of an apparently cartilaginous structure, occur a little in advance
of this. These were probably the bones of the head, and one of them contains several teeth.
The scales were very numerous, and, from being closely connected with the fin, are consi-
dered as belonging to the same animal. No other remains were found in the same situation
in the rock. .
The remains figured in this plate and the woodcuts above, are all from near Blossburgh,
Pa., none being found in the Fourth District of New-York in sufficient perfection.f -
* A notice of this fossil was read before the Albany Institute in 1840, in which the name Sauritolepis was proposed, and I
afterwards published it under this name in the Annual Geological Report. Being at that time desirous of founding the generic
distinction upon the scales, in accordance with the system of Agassiz, I overlooked the more obvious character of the fin. Since
this has never before been figured, and the name probably not adopted, it will give rise to no confusion by changing it to Saurip-
teris, from the sauroid character of the fin.
# I had felt disposed to wait the appearance of the Geological Report of Pennsylvania, by Prof. H. D. Rogers, before giving any
figures of these fossils; but on consulting him, he, with his usual liberality, expressed not only a perfect willingness, but a desire
that they should appear in my report, as they were obtained in extending my examinations beyond New-York, to a more perfect
exhibition of the Old Red sandstone in Pennsylvania. - .
OLD RED SANDSTONE, 283
Thus far we know little of the fossils of the Old Red, but, from the rich harvest of these
cursory explorations, it may be expected that we shall yet bring to light a much greater
number of species; and if we are not able to compare in number and singularity of forms
with the fishes of this rock in Britain, we may, perhaps, discover others which will throw
new interest around the investigations of the Old Red Sandstone. The Sauripteris, if I am
correct in my inference regarding its structure, enables us to extend the Sauroid type to a
lower position than heretofore ; and from what has been remarked under the description of
the lower rocks, we are now able to extend the evidences of the existence of fishes to a
lower point in the system than has ever been previously done. -
36°
284 GEOLOGY OF THE FOURTH DISTRICT.
Sºº assºs
§§§
§ &
| W: ſº Šćغ gº
tº { % s Fº
§ à º
Wº:
º
§§ lsº
* † $º N.SYS &S º \\, *
§§§ § Fºsº
#% * §
§§. # %ft §§§ ºž
§. # É: §§ ºft ſ # * if, jº % -
ÉÉ #sºft#3;
§ * º š. : É º/
ºš Higº.º: ºº:: ###### FS:ESSºFS * *
sº #sº - É$#4432.
Sºº-ºº: % ſº->\|\; - - º-º º
§º
C.- s:==3:3:=$º | ſº -
- -- - S. *~ s:- 4-gº
E--->
º-sº
Sès - N *s
- N ~
- - &- ū § =>s- •
wº º: N- 2 , -’ ºak-
E=\;= E-3 cºſtill mº-->
- º E- *
--r-º-º-º: .
*º-ºº-
E=º
WN
---
º à- Eº º
- º:
#
y
ºr.:
gº
º:
§
==== - S:
w - º lº ~ . -
~\ºs Nºş tº
N M-º. wº- * § w &# āşş izºſº * - gº • .
ºr sºjº £ºãº S㺠5:3
v - §§S #º E ==S ſº :…:* -
--~~~~ a lºº
šºs::===5°º
#####2;&A
% =#=%
**-ºs- Éc. - : .* .
:::::::::::::::: ºr ººº-º-º:
º:-----º-º:
..º...… sº
E:ºz.T. - Tººwº " ...:”.
꺺::::::::
&: ...l. ºrsºvº
- Tº: - # s:
- ºx=> * * slºº
>E::=> ==ºf -> Iſº 2. 2- - 㺠º: - :
- - - ==<==ES:ºx º'cº-º-º-º-º-º: z_---->~~~~~~~~~~~…it iſºtº º à . . .----. --~~
r_>~Tºs::=>:::::::::NT - T. z====<: ---~~~~\!"..…! ºw- sº º-: -
* . =#=#===º Nº.2º:2:…------ºº: Sºcºs ºccº.º.
F.s: --> == ====} ……ex-->~~~~~ º sº..…” N. ~...a…a…aaoº---—zzee
~:=== == §:=== - afºgº &=## ><ſº - &zºg
s -- ====ºs Sºº-ºº::=ffº. #|ſ; § -->====##### T.--~~~
-- #### sissis; ###!ºãº -wºº
|-º:És §lºse==# iº #|}}} ºëºlº. ... • * ... ---sº a * * gººses
~~ cºº a- º - 5- - º :ºx. - *** ***. * * * -
** ==::=::=>==== £º: Eºllº EE#####|||}= Mø--
- - - -º- Þº tº:--º-- ****--~~~~ º - šft||| }*-2"
sº Băsº º: i.--
ºxº-ºº::
=ºsosº
§ -> 2:… "
- sº
*º- Erºs: gº ºrz-->2-
- S-ºº-º-º: z-z
z_2=-&###2: ^2,
--—-->
3-º-
Sketch of the northern edge of the Conglomerate, six miles South of Olean in Allegany county. By Mr. E. N. HoRSFORD."
CHAPTER VII.
CARBONIFEROUS SYSTEM.
CONGLOMERATE, OR EQUIVALENT OF THE MILLSTONE GRIT OF ENGLAND.
Under the term Carboniferous system, it is intended to include all those deposits which are
considered as belonging to that period in which the great coal-fields were produced. These
are marked throughout by characters which indicate a certain prevailing condition in the ocean
and the nature of the deposits, and a similarity in the nature of the organic products. All the
workable coal seams of the country are confined to this formation, and none have ever been
known to occur in the rocks previously described in this Report.
* The illustrations of this chapter, and that upon jointed structure, were mostly sketched by Mr. Horsford,
CARBONIFEROUs systEM. 285
The second member only of this system is known in New-York; and from the situation in
which it occurs, little of interest or importance can be expected from it, except as showing the
remains of an important formation, which once extended widely over the southern tier of
counties, but from subsequent operations has been almost entirely removed, leaving only the
isolated fields and blocks which indicate its former extent and importance. -
The Old Red sandstone in the Fourth District, is succeeded by a coarse siliceous con-
glomerate, and a grey diagonally laminated sandstone, the former generally prevailing. The
conglomerate consists of a mixture of coarse sand and white quartz pebbles, varying from the
size of a pin's head to the diameter of two inches. They are generally oblong, or a flattened
egg shape. Some of these are of a rose tint when broken, but white upon the exposed sur-
face. Pebbles of other kinds are very rare in the mass, though red and dark colored jasper
are sometimes found.
This rock in the Fourth District occurs in outliers of limited extent, capping the summits
of the high hills toward the southern margin of the State. It is represented on the map by
small dark spots, and its relative position is seen by an inspection of the sections crossing
the counties (Plates 10, 11 and 12). From the absence of the red shales and sandstones
forming the Old Red, this rock, on the west of the Genesee, rests directly upon the Chemung
group. . - . . .
From its position, it has been much undermined; and separating into huge blocks, by
vertical joints, which are often many feet apart, the places have received the name of ruined
cities, Rock city, &c. The sketch at the head of the chapter will give an idea of the cha-
racter presented by this rock in its exposed edges. In many situations it can hardly be con-
sidered as being in place, the wearing away of the rocks beneath having allowed the mass to
fall down, so as to occupy the side of a hill instead of the summit.
It is often much broken, and scattered fragments extend on all sides of the principal outliers
to considerable distances. In many instances I have detected huge fragments of this rock
nearly as far north as the northern limit of the southern range of counties, lying on the hill-
sides, and sometimes in the valleys. At first I was disposed to consider these as transported
from the south, knowing no rock in place of the kind so far north. Subsequent investigations,
however, have convinced me that these fragments are the remains of the rock itself, which
once extended continuously much farther north than its most northern outliers at the present
time. . - -
In some instances, we find perhaps but a single mass; again we may find several, and in
a few instances I have found a long range of fragments flanking the southwestern slopes of
hills, and a similar arrangement upon an eastern slope, and again upon the summit of a broad
flat table land surrounded by higher hills. These fragments have all the characters of the
rock in place, and some of them occur in the immediate vicinity of such localities, and in one
or two instances to the south of points where the rock is known in place. The occurrence,
therefore, of single fragments, or of several in proximity, in the southern counties of the
286
GEOLOGY OF THE FOURTH DISTRICT,
district, must be regarded as evidence of the former existence of the rock at these points, or
farther to the north.*
In some places where this rock is a sandstone, the marks of furrows and striae are still
clearly preserved upon its surface; showing the influence of that denuding agency which
removed the greater part of the rock, and probably the same which excavated the deep valleys
crossing this part of the country from north to south, as well as many lesser ones in other
directions. The prominent outliers of this rock upon the high and distant hills furnish good
landmarks for showing the extensive denudation which this part of the country has suffered.
From its great extent northward, it appears very probable that originally some of the lower
beds of the Pennsylvania coal-fields extended into New-York, and that being of more de-
structible materials than the conglomerate, they have been entirely swept off. This may
appear more reasonable, when it is stated, that about six miles south of the State line, on a
high ridge of land between the Allegany river and the Connewango creek, a bed of coal lies
upon the conglomerate, which latter extends thence northward into New-York, its broken
outliers appearing for ten or fifteen miles north of the State line.f
Wº -
º
*
|
§§ |
*...[
º
Diagonal lamination.— The diago-
nally laminated structure is often beau-
tifully presented in the broken cliffs and
large fragments of this rock, and this is
one of the most obvious characters.
The illustration No. 133 is of a quarry
at “Burned hill,” in the south part of
Allegany county. The alternation of
horizontally laminated strata shows the
varying conditions of deposition. The
stratum below the upper one shows an
undulated structure very much like the
rippled surfaces, but not so well defined.
Tºº-ºº----------.
tº
*
ill
*-
-* -—-
-] º rº-ºst sº: E --
º: - - ---
=#5
--=ºs:
-]
*
= 'º - Re-
sº º
== sº | sº iſiº ==<
E=# º ºf E==
#ºf H -
Diagonal lamination in sandstone.
* I am frequently reminded that these huge fragments, scattered upon the hills in this manner, are the loads deposited by
immense icebergs, which have here stranded, and subsequently melted away. But however plausible this argument may be, I
prefer another solution of the phenomena, which appears more in accordance with facts here given. Although this would show
a former extension of the conglomerate to points twenty miles north of where it is now known in place, the inference seems
unavoidable, and well substantiated.
# The points where these striae and furrows occur are on some of the highest hills in Chautauque county, and nearly two
thousand feet higher than similar markings along the borders of Lake Ontario. - -
# There is another conglomerate in Chautauque county, and in some places in Allegany county, which was briefly noticed under
the Chemung group. This, however, is a thin mass, and wherever it has been found in place, is associated with fine-grained
compact sandstones, and frequently contains the fossils of the Chemung group. In the northern part of Chautauque county, I
found some loose masses of this conglomerate, containing fossils known to belong to the Chemung group, and by this they were
chiefly identified. The aspect of the rock is also somewhat different; the pebbles smaller, more round, and not of the same white
quartz which occurs in the higher rock.
CARBONIFEROUS SYSTEM. 287
At this point the conglomerate was not seen in situ, though numerous fragments were found
upon the slope of the hill. * -
The following is a section showing a similar structure in a block of conglomerate in the
“Rock city,” south of Ellicottville.
s-ºº-º-º-Eº “Tº
z-s:
|| || | | ſº || | º
# =&ºts= | hºmimſ | || || ji====
E. : * ~~
iº-º: sº
==
§
------ #}}|
|WWii Nº. º º
º |||||||||f|| tº º Hºss
|Éiº
º
Concretions and seams of iron ore.
In many places this rock is traversed with seams of iron ore, which often stand out from the
surface of the blocks, having resisted the influence of the weather which destroys the mass.
These seams are sometimes in right lines; at other times, undulating; and rarely, if ever, in
the direction of the lines of deposition. They are evidently segregations from the mass, and
the irregular and undulating direction is due to accretionary force. In some instances, nodules
of hydrate of iron have been found; at other times, the folded seams or laminae enclose a
mass of sand, which has apparently resisted the formation of a solid concretion of iron ore.
288 3EOLOGY OF THE FOURTH DISTRICT.
The illustration above exhibits these seams as they appear in two blocks of conglomerate at
Rock city. The seams are an inch thick; the lower one at the left hand folding irregularly
around, and enclosing a portion of sand : the same concretionary tendency is seen in a part
of the seam on the right hand side. J. - -
The illustration No. 136 represents a thicker seam of the ore upon the surface of a loose
block, where the weather has removed the rock above. This shows a tendency to folding,
as in the other instances. Small nodules are sometimes found, though rarely, which do not
enclose sand.
136.
—====== ======= ====- .
H
a ºffl
-
l
| º †
\\\\\\（
º
º
|
cº-
a. 8 ºfflº-E:
> frº-E
Eºsters--> -
- º-º-º-º-º-º:
&-ºm-º-º-º-º-º:
::::::::::=ºffl Eº:=: #===#:=
**** *** º -->==-3:
:=º:=-º:Br:#E
:=º-E::==E
º-ºº::==E.E.
- E--->
al-º-º-º:
tº-º-º:
† -------º-º-º:
-------Tº-ºº:E E- w
The existence of these seams, and the concretionary structure is noticed here, from the fact
that farther westward, small concretions of ore, and concentric seams similar to these, are of
frequent occurrence, and seem to characterize the mass. -
At the Cuyahoga falls in Ohio, the cliff of conglomerate presents some interesting exhibi-
tions of these seams, which the following woodcut illustrates:"
137.
1 2 3
Fig. 1 is an example where two centres are formed, which are subsequently enveloped by concretionary laminae.
Fig. 2 exhibits concentric rings or laminae, which expand farther upon one side. - g
Fig. 3 presents irregular concretionary or concentric laminae, enclosing a few undulating ones, but with no well defined centre,
* See Transactions of the Association of American Geologists and Naturalists, Vol. 1, 1843.
CARBONIFEROUS SYSTEM. 289
/f
Localities.—The first evidences of this rock noticed in the district, were in Chemung
county, where a few boulders and fragments were found. The same were observed in Steu-
ben county, at several points; but the rock was nowhere found in situ. In Allegany county,
there are several places where appear the remains of the mass, and which hold their original
position. One of these is near Wellsville, on the Genesee; a second is in the town of Scio,
about five or six miles west of the former. The first point presents only the diagonally
laminated sandstone, with loose blocks of conglomerate; the second is a coarse conglomerate,
the finer parts of which have been used for millstones. - -
There is another locality still farther west, in the town of Little-Genesee, where the rock
is of the same coarse character as in the last. - - -
About six miles south of Olean,” and nearly on the State line, there is a tract of several
acres occupied by this rock; its northern outcropping edge is much broken, and huge masses
are scattered for a mile or two around on the slopes. Some of the blocks, where the rock
lies apparently undisturbed, are sixty or seventy feet long and thirty or forty feet wide, and
so widely separated by vertical joints that they offer spaces like streets and alleys, converg-
ing as we approach the rock in place. Sometimes the roots and loose vegetable soil has
extended over these fissures, and they then present covered ways which often lead to the dens
of wild animals, and which, in the early settlement of the country, were tenanted by bears
and wolves. At present, except in rare instances, the fox and hedgehog appear to be the only
occupants of these places. - -
There are several points in Cattaraugus county where the conglomerate is very well exposed
upon the tops of the hills. The best known of these is the “Rock city,” about seven miles
south of Ellicottville. This place is upon the top of a hill, about two thousand feet above
tide water. The situation is very similar to that south of Olean; the blocks are widely scat-
tered along the margin of the hill, and as we approach the undisturbed parts of the rock,
they become more numerous, and soon assume a regularity in arrangement which shows them
to remaih nearly in their original relative position, except that the joints are widened by
the undermining of the rock below, and partly, perhaps, by the destruction of the rock itself.
The whole presents an appearance like a cliff of harder rock resting on a more destruc-
tible one below, which has been exposed to the waves of the sea or large lakes, examples
of which are presented on a smaller scale in some of the sketches along Seneca lake. In
some places where the blocks are otherwise closely arranged, there are large spaces, where
the masses have been removed or disintegrated, presenting a fancied resemblance to court-
yards or squares in the midst of the numerous streets and alleys. The whole area occupied
by the rock at this place is estimated at an hundred acres, though the space where the rock
is not scattered is not more than half this extent. -
The sketch below represents a few of the immense blocks at this place, with the passages
between them. The large trees which stand upon the top, have often sent their roots down
* See the illustration at the head of the chapter.
[GEoL. 4th DIST.] 37
290 GEOLOGY OF THE FOURTH DISTRICT.
the sides, where they are sustained in the deep soil, supporting the huge growth above upon
an almost barren rock. * -
138.
§§§
º [-3
i.: 5 NSS-_ -a-ºº:
iſjºº 3. §: § - Y:=t -- . -->. º §§ §s. _* • ? cºs; %lſº º
ſºft ſº ºğ. §=_ ºft §s —ºr º% SNN-
% # \\{º É=:: #% º §§
J|| º º ſº zºº % §§§
re .. ſº ºf ſ słº, f º - &/º §§ º:
§ | % # 㺠§§
§l | §h Sº §§ º - § *S**
gº +: Gº: #= º º:
:- §§
:8
w §§§ º
§§§ § :
** §§§ º º
* º
sº
|; #
#||
º
º § º seasº º - ſº § *-*.
º - ºf ºi... • * * v {ij} ||
º
- š
y-ll-JT º ºgº
|-(-)-l' ' || 1: | --~~~ ºft|||
| º) || Iterº #º º - | |
º
jº
|
|
|
§§§º:#####|ſº ÉWº * * ### ºffſ
| º Rºssº # º
Sºº š sºHº º º | ſ º
cº-º-º-º: *-
º º ~~ *== º
5 iſfy ſt ji º | §º
| | |W
|||ſ|}}}|||}^3|||||||}|
ſº. rº-rºxi §
#ººse
View in Rock city, Sévén miles south of Ellicottville. From a sketch by Mr. E. N. HoRSFORD,
The masses present the same features as before described, and offer fine exhibitions of
the diagonal lamination and contorted seams of iron ore. The rectangular blocks are from
thirty to thirty-five feet in thickness, and standing regularly arranged along the line of out-
crop, present an imposing appearance, and justify the application of the name it has received.
Near Judge Wright's, a few miles southeast of Ellicottville, the conglomerate appears on
the tops of two hills, separated from each other by an east and west valley. It also appears
between Napoli and Little-valley, and at another point between the latter place and Great-
valley. There are also several places on the south side of the Allegany, where it appears
on the tops of some of the highest hills. In all, except two or three of the localities enume-
rated, the rock appears in scattered blocks. - -
In Chautauque county there are numerous localities where this rock appears, either in situ
or in scattered masses. It is frequently nearly free from pebbles, and furnishes a good quarry
stone. The principal places where it has been quarried, are upon the top of a hill two miles
west of Ashville; at Williams’s quarry four miles north of Panama, and at another place
one mile north of the latter. At Panama, the conglomerate in huge masses lies along the
eastern slope of the hill, and upon both sides of the stream. It rests upon the soft green shale
CARBONIFEROUS SYSTEM. 291
of the group below, and has evidently been thrown down from a higher elevation by the
removal of the rock beneath. The masses are sixty or seventy feet long and of equal thick-
ness, having a breadth of thirty or forty feet. The rock appears to be nearly continuous,
separated only by fissures of greater or less extent and width. - .
All the localities known in this county were enumerated in the annual report of 1841; and
they are all indicated by the dark spots upon the map. -
Thickness. – The thickness of this rock varies at different localities from twenty-five to
thirty-five feet. At Panama it is about sixty feet thick, and this is the greatest thickness
known in the State, though a short distance south of the State line it becomes one hundred
and fifty feet thick. The varying thickness may arise from original inequalities, or from
denudation, which has operated unequally in different places. In many localities where the
same rock appears in Ohio, Indiana and Kentucky, the thickness is nowhere greater than one
hundred feet. -
This rock, for the most part, occurs on the high grounds which still remain entirely uncul-
tivated; where, however, the land has been cleared of the forests, it is unfit for cultivation,
but it is equally valuable for the building and underpinning stone which it furnishes, there
being few other rocks in that region which are fit for these purposes.
Organic Remains of the Conglomerate and Sandstone.
Fossils are extremely rare in this rock, having been seen in one locality only, and in this
the sandstone predominates largely over the conglomerate. Beyond the limits of the State,
vegetable fossils are of frequent occurrence, though but a few imperfect fragments have been
seen in the Fourth District. -
3-
1. Euomphalus depressus. 2 and 3. Cypricardia? rhombea. 4. Cypricardia contracta.
1. EuOmphalus depressus, Il, S. —Depressed-spiral; lower side broadly concave; whorls,
about three, round. -
This fossil closely resembles the E. serpens (PHILLIPs, Palaeozoic Fossils, pl. 36, fig. 172).
2 and 3. Cypricardia? rhombea, n.s.-Sub-rhomboidal; oblique; beak prominent; shell
smooth. -
37+
292 - GEOLOGY OF THE FOURTH DISTRICT.
4. Cypricardia contracta, n. S. – Oblong, sub-elliptical, very inequilateral; contracted in
the middle; surface marked by concentric wrinkles, which are stronger toward the anterior
margin. - - .
Locality—The three species here figured occur at a single locality about four miles north
of Panama, Chautauque county. t.
Along the northern boundary of Pennsylvania, this conglomerate forms the margin and im-
mediately underlying rock of the coal measures. Tracing it westward into Ohio, we find it
there holding the same relative position to the rocks of New-York, and to the coal, that has
before been shown. The absence of the Old Red sandstone brings it directly in contact with
the Chemung group below, over all the western part of New-York, and it holds the same place
in Ohio at all localities examined. As before remarked in the last chapter, the intervening
strata which separate this rock from the Chemung group are absent, having apparently never
been deposited over a very large tract of country. Its outliers in the Fourth District offer
less satisfactory sections than the same rock when more continuous. .
The following section at Cuyahoga falls, in Ohio, exhibits the relative position of this rock
and its associates.” -
140.
~ T-
T-
— — 3
-T--—
22% tºº.2324,72) º .7, e
--~~~
Ežzº A V, tº: Zz-z-Z Zºº.
22.2% “Jºž 2%//*
~ += −-\_A= − = F-
- l
*-
1. Chemung group. 2. Conglomerate. 3, Coal measures. A. Channel of the Cuyahoga.
The river bank presents the two lower rocks in connection, and the coal beds with shales
and sandstones occupy a slope extending eastward from this point. This is near the western
extremity of the coal-field; and when we next meet the conglomerate in a western direction,
we find it resting upon a limestone, and its relation to the rocks of New-York is illustrated
in woodcut No. 129 on page 280. - -
The conglomerate still holds its relations to the coal measures as before, forming the
eastern and southern margin or edge of the Great coal-field of Illinois and Indiana, which
likewise extends into Kentucky. The same rock forms the western margin of the Ohio coal
measures throughout the State, and extends north and eastward, as just mentioned, bordering
the Pennsylvania coal-fields; and Prof. Rogers remarks, that it also extends into Maryland
and Virginia, holding the same relative position. These facts are of the highest interest, both
in an economic and scientific view ; for since its extent is so well marked and widely known,
it may, in all places, be relied upon as indicating the proximity of coal.
CARBONIFEROUS SYSTEM. 293
From its relative position to the coal and the lower rocks, I had inferred that it was the
equivalent of the Millstone grit of England. The presence of the great limestone formation
beneath it at the west, still further sustains this opinion; but since we know perfectly well
its relations to our own rocks, both above and below it, its identity to, or difference from,
foreign rocks, is of less consequence. - -
The section, Plate 13, illustrates the relative position of this rock and its associated strata,
both as regards the eastern and western coal-fields. The series, throughout the Fourth Dis.
trict, is so little disturbed that there is not the most remote possibility of a coal bed being
found in any depression or fault of the strata, and vague surmises and useless explorations for
this mineral will doubtless soon cease. - - -
Since it is well ascertained that coal of the true coal formation does not exist within the
limits of the State of New-York, it may be well to state here, for the benefit of my readers,
the position in which this mineral has been sought. The dark shales and shaly sandstones
of the Hudson river group and the Utica slate, are the lowest positions which have been ex-
plored for this mineral. Along the Hudson river, as already stated in the annual reports of the
First District, there have been immense amounts expended in search of coal. In the Fourth
District, the lowest rock in which it has been sought to any extent is the Marcellus shale,
and above this the Genesee slate, and various parts of the Portage and Chemung groups,
particularly where the slate is black and highly bituminous. Thin seams of coal do some-
times occur in these situations, but they rarely extend beyond a few feet, and are usually less
than an inch in thickness. -
These seams or strings of coal are not indications of its existence in larger beds; and the
lithological character of the strata, though ever so similar to that about coal mines, cannot
alone be relied upon. In all situations where coal beds occur, the shales and shaly sand-
stones contain the remains of land plants, like ferns, often in great abundance; and the
absence of these in strata, with the occurrence of certain marine fossils, may be looked upon
generally as conclusive evidence of the absence of coal. The organic remains of these
strata thus become of the utmost importance in identifying their position; and those forms
previously figured as marking rocks below the coal, will always be found in the neighborhood
of any excavations made in the rocks of the Fourth District. This negative knowledge of
the absence of coal in the State is of the utmost importance; for although it may not enrich
the possessor as much as a coal mine, it will still enable him to avoid a useless and wasteful
expenditure in search of that mineral. - º-
The reasoning, or rather assumption, with which my arguments and facts are often met,
particularly in the southern counties, is, “Why may we not as well have coal in our hills,
as they have in Pennsylvania * “I am sure there must be coal, or some mineral, in these
hills, for they are good for nothing else.” The reasons why coal does not exist in these
hills, is already shown to be because they hold a lower position than any rocks which contain
coal in workable seams. That these hills are fit for nothing else, I beg to dissent; for by
proper treatment in their cultivation, and the use of means within the reach of every farmer,
294 GEOLOGY OF THE FOURTH DISTRICT.
they may be rendered the best kind of grazing land, and produce all other articles required
for the support of man. So long as the belief exists that there is mineral wealth in these
rocks, so long will the cultivation of the soil be neglected, and consequently the country will
remain unproductive, not because the Creator made it so, but because man has proved an
unfaithful steward. - - - -
In these situations, as well as in all others, there is room enough for rightly directed enter-
prise; and a knowledge of what does and what does not exist, is of the utmost importance in
guiding that spirit which has built up the thriving village, the lofty spires of the city, or spread
the widely cultivated farms where the primeval forests but lately held dominion, and which,
even to the remotest bounds of civilization, is drawing from the earth treasures richer than
the gold mines of the south. - - - -
These show to us that our favored country, even in its widest extent, possesses prečminently
the means of ameliorating and exalting the condition of mankind, and of promoting the arts
of civilization in the highest degree. It is a wise arrangement, that those things which we
prize highly should not be placed within our reach at every point, for they would soon cease
to be valued. A variety of pursuit and production are necessary to the welfare and improve-
ment of man, and the surface of the earth is so adapted as to compel this diversity of pursuit;
and man, whether he will or not, submits to the laws imposed upon this earth and all its
created beings. And although in some points man may reason that himself, or his neighbors,
or his posterity might be benefited by a different arrangement of what he considers the rich
or the desirable things, yet he is to remember that himself and those around him form but a
small part—a link in the great chain of community, which is ordered and governed by laws
which emanate from the great source of all order and harmony in the universe.
UPLIFTS, DISLoCATIONS, etc. . 295
:===#
===== -- ---
E---> * ºrº- a- ~ -
e------>= E==:: *:-º Eºs:->=
:=#=== #======E >
==#############
# =#==== -
E. E
- - - º
a-
Uplift in the strata, two miles above Eighteen-mile creek,
CHAPTER VIII.
Uplifts, Dislocations and Undulations of the Strata in the Fourth District.
Situated as the western part of New-York is, mostly remote from any known rocks of
igneous or hypogene origin, there are, as we should naturally infer, but few of those dis-
turbances which manifest themselves along the margin of mountain ranges, or the vicinity of
intruded rocks. Those which do present themselves are of little comparative importance,
except as illustrating the extent of this force, which, in other places, has produced phenomena
of the most stupendous kind. - a • -
The existence of trap dykes upon the immediate borders of the district, show that the
dynamics of igneous agency have not entirely slumbered. The undulations which extend,
like immense waves, over the whole breadth of the district, show also the influence of some
subterranean agency which converted the rocks into a billowy sea. -
The manifestations of local disturbance, whether from deep seated causes or from some
local operation, are confined to a few slight upliftings or dislocations of the strata; sometimes
an abrupt flexure marks the point of the application of force, where the strata have not been
broken. The figure at the head of the chapter represents a slight uplift of the strata at the
upper part of the Hamilton group. The thin mass, which is the encrinal limestone below the
Moscow shale, together with this rock, is abruptly elevated about four feet. The limestone
has been broken suddenly off, while the shale, though less sharply broken, is, nevertheless,
296 GEOLOGY OF THE FOURTH DISTRICT.
plainly fractured, and the small fragments in the joint are crushed and partially ground to
clay. The amount of lateral motion may have been greater than appears; for an oblique
fissure, extending from the vertical one to the left, was found to have the surfaces striated.
Such a phenomenon could scarcely have resulted, unless from the moving of one surface
over the other, by a lateral force. - *-
Beyond this point, in a southwest direction, the dip continues as uniform and gentle as on
the northeast.
Several other points along the lake present similar appearances. The following occurs a
few miles northeast of the Pennsylvania line, in rocks of the Portage group.
142.
º
ºt w
º
º
º
§§
xt
Elevation and fracture of the strata. Ripley, Chautauque county.
The strata are mostly shales, or shaly sandstones, with a single thick bed of sandstone,
which is broken at numerous points along the curve. The irregular fracture is strongly
stained by decomposing pyrites; and there seems to have been injected mud, which has
forced its way into all the fissures and between the shaly laminae, for several inches, and often
for several feet. The laminæ of slate and shaly sandstone are broken, and stand in the frac-
ture at various angles, from nearly horizontal to vertical. • ,
The fracturing of the strata has rendered the mass much more destructible, and the waves
have worn a deep, cavernous depression, which recedes fifteen or twenty feet beyond the
general line of the cliff. Many of the indentations along the shore are produced in this man-
mer, their commencement being the fracture in the strata. I have seen several where the
amount of excavation is much greater than in this, but much of the same character.
UPLIFTS, DISLOCATIONS, etc. . 297
In other parts of the district these uplifts have produced lines, which, being more easily
excavated, have become the channels of streams. Many beds of streams present this appear-
ance, but in most cases I have been inclined to refer the apparent phenomena to very partial
uplifting of the strata by ice. Very many instances are doubtless due to this latter cause;
but there are others which cannot be referred to such an influence. The following is a
section of the south branch of the Cattaraugus, with an elevation of the strata upon either
side : - -
The disturbance is here so great, that it seems due to some more powerful agency than
the freezing of water. Still, however, so many points present similar appearances, which
are evidently due to the latter cause, that it is not easy to decide.
This effect of uplifting is sometimes manifested only along the line of fracture; the strata,
on either side, manifesting the same line of dip as if it had not occurred. The following
illustration is from a cliff on the south branch of the Cattaraugus, one and a half miles above
Little's mill. The strata on either side of the line of fracture are apparently as undisturbed
as if it had not happened. -
[GEol. 4th DIST.] 38
298 GEOLOGY OF THE FOURTH DISTRICT.
144.
=ſ.
==
=%
-.
|
%
ſ
| AS
º
İ
|
**** ---
E--->
F===>=EE
E---> F-
-º-º: -
-º-º-
EEE--->
*- >=>
- ---E
- *
=======#
#sº º-E-E-S
- = -
==# - z: *T*- = *-Tº-T-TE ss===
======E=== 㺠=======
==EE--- Tillſ||ſiſſiſtſ' # ==-”
- - - ºsº ºfflººs-->
z-> --> º-º-º-º-º: Ecº
There is an oblique line of fracture, as represented, ascending to the left; and this is a
common circumstance attending nearly all these fractures or dislocations. It will be per-
ceived that the amount of dislocation is never so great as to produce any evidence upon the
surface; and these localities are only interesting as showing the influence of causes which,
at other points, have wrought such mighty changes. In every instance which I have observed,
the direction of this force is at right angles to the line of dip, or in the direction of the out-
cropping edges of the strata. It is in the same direction mainly that the great undulations
extend, and both are probably due to the influence of the same agency.
Besides these fractures and dislocations, others appear to have a local origin, such as the
downheaves along the line of dip in the limestones. In tracing the limestone southward in
Seneca county, we find its dip, often greater than the average of the strata in other places :
and after its disappearance, we again find the same layers rising to the surface still farther
south. Although the soil covers the surface, and the absolute fracture is not seen, yet it
doubtless exists, and is probably due to the falling down of the layers on the north, from the
removal of the soft marls of the Salt group below." p
The same layers appear at the successive points 1, 2, 3, or at least they are so precisely
similar that there is no possibility of distinguishing them; and we farther know, that if the
thickness of the rock is estimated from adding all these successive outcrops, it would be
greatly increased over the same in other places. -
* See illustration, page 163.
JOINTED STRUCTURE. 299
º
C-
**T*-as-s-, *-3-
---->
-
*
--
wº
É
É
É
===Tº
a---------
--tº-
W
---...--
=\
-
---
--
º
-
&
º
tº:
tº:*-
View of the Cliffs on Fall creek. From a sketch by Mr. E. N. HoRSFORD.
CHAPTER IX.
Jointed Structure of the Rocks of the Fourth District.
In addition to the slaty cleavages which separate the rocks of the Fourth District into
laminae parallel to the planes of deposition, and those lines of separation which divide the
siliceous and calcareous masses into thicker blocks, we have another series of divisional
planes, for the most part vertical to the line of deposition, and often penetrating to great
depths, as seen in high cliffs and river banks. These lines of division have two directions,
crossing each other, generally, in slightly oblique angles; though there are cases where the
direction is nearly rectangular, as in the conglomerate, which is divided into huge blocks,
often separated several feet from each other. -
Where these joints are numerous, they divide the rock into blocks of convenient size for
quarrying, with vertical faces of great regularity; and where the blocks are too large, they
38*
300 GEOLOGY OF THE FOURTH. DISTRICT.
are readily split in a direction parallel to the natural faces. These vertical divisions are of
immense importance in quarrying, particularly in the limestones. I have seen quarries
wrought to the depth of twenty or thirty feet, and for several rods in length, the back formed
by a single plane, or by the salient and reëntering angles of the lines of these joints. Owing
to this circumstance, a great amount of labor and expense is saved over what would be neces-
sary if the whole length and depth was to be wrought down by blasting. -
In cases of slight disturbances or upliftings of the strata, as there have been in some places,
the slaty cleavage seems more perfect, and the joints more numerous as well as better defined.
146.
Section on Twenty-mile creek.
In this instance, from some cause or other, the joints are exceedingly abundant; and they
are not all vertical, but cross diagonally from one to another; neither are the planes all parallel
in their horizontal direction, frequently meeting, so that the block between them wedges out
at a very acute angle. - *
The same formation of rock has, in one place, a more perfect jointed structure than in
another, though there has been no perceptible influence exerted. Still, however, it may be
due to similar causes, and only at a greater distance from the centre of influence.
These joints, though usually perpendicular to the planes of deposition, or slaty cleavage,
(which are coincident,) are not invariably so; they are sometimes oblique to this direction,
and even curved, leaving a spheroidal surface upon the mass below as the upper becomes
removed. * - - - -
Notwithstanding that joints are far more numerous in the vicinity of slight uplifts, still I
would not infer from this fact that they are due to the same cause. The manifestations of
disturbing influences at such points may be owing, as suggested by Prof. Phillips, to their
presenting less resistance than others; and for this reason, though the force were applied
equally under the whole area, that point where joints were most numerous would yield first.
It becomes a subject of interesting inquiry, why certain shaly masses are destitute of this
symmetrical division, while others of the same age possess it in a high degree; for so far as
external appearances are concerned, they are as susceptible of such effects as those where this
structure is perfectly developed. Several modes of explanation offer themselves to account
JoINTED STRUCTURE. - 301
for these phenomena; but future observations are required, before any satisfactory hypothesis
can be advanced. ^ - -
From all the facts observed, there seems reason to believe that these joints are due to
galvanic or magnetic agency which has pervaded all the strata; but that certain subterranean
influences, operating at certain periods or under certain circumstances, may affect this con-
dition. Where such an agency has acted more powerfully over a limited area, it may have
produced a greater development of this symmetrical structure. The fact that these joints for
the most part follow a uniform direction, points to some universal law like galvanism, or
pervading heat, as the primary cause of their production. The uniform direction of metallic
veins is not more persistent than is the direction of these joints; and if we refer the cause of
the former to galvanic agency, why should we not refer the latter to some influence equally
universal? - - - r
The tendency of our ordinary clays to separate into laminae parallel to the lines of deposition,
and also by vertical planes into rhombic masses, indicates the same structure, and the operation
of the same laws as those producing more extended effects upon our slate rocks.
The shores of our lakes, the banks of rivers, and the high cliffs bordering the ravines of the
southern counties of the district, present these joints in great perfection. The whole effect
produced by them, the sliding down, the undermining and destructive action of the weather,
is picturesque in the highest degree. In some places, their great number and regularity
suggests the idea that they may have been produced by causes not unlike the symmetrical
divisions in the trap and basaltic rocks. This effect, though not as regular as the latter, is
often nevertheless constant in certain rocks, and as equally governed by certain laws, and we
may not unaptly term it mountain crystallization; yet, although we cannot prove that the
ordinary laws of crystallization have had the slightest influence, so neither can we in the
columnar basalts. In these we find the direction of the columns at right angles to the cooling
surface; and in the jointed structure, we find, with few exceptions, that the direction is at
right angles to the plane of deposition.” - -
From the smoothly vertical faces of these joints where the rock is of a uniform composition,
we are compelled to ascribe the cause to something beyond that which contraction on desicca-
tion would produce; indeed, from analogous cases, this latter kind of structure is not produced
in right lines, but in variously curved and undulating directions. Another objection to this
latter view is presented in the fact that some of the most argillaceous masses, or those which
on desiccation would contract most, are nevertheless almost or entirely free from these sym-
metrical divisions. Limestone, on the other hand, which in many cases we must suppose was
+ Sandstone in conjunction with trap, often becomes columnar for a distance from its point of junction with the trap; and I
have seen fragments of furnace hearthstones, which had become columnar in like manner. In these cases, we cannot doubt that
this columnar arrangement has resulted from the action of the heat upon the sandstone. The jointed structure is often very
analogous to this; and in the vicinity of slight upliftings of the strata, the joints cross each other so closely as to give the mass,
where partially broken or removed, a columnar appearance. Granite or gneiss often takes upon itself this columnar aspect so
perfectly, that at a little distance it might be mistaken for columnar basalt.
302 GEOLOGY OF THE FOURTH DISTRICT.
produced by corals, and often much crystallized, being in a condition to exhibit less of these
divisions on desiccation, is nevertheless always strongly characterized by a jointed structure.
Slates, also, where the laminar structure is well defined, have always this jointed structure in
great perfection; while in those where the slaty cleavage is not observed, the joints are like-
wise very obscure, or but imperfectly developed. Although there may be no sufficient reasons
to induce the belief that one is dependent upon the other, still, in rocks of similar composition,
where one is absent, the other is likewise. - -
In many instances we find a fossil perfectly divided by a joint, the respective portions re-
maining on either side of the fissure. Numerous instances of this kind may be seen in the
plane of a single joint in the fossiliferous portions of the Chemung group. Had these joints
been due to any thing like the cracks in ordinary clays, or those produced during desiccation,
it is hardly possible that these fossils would have been divided in this regular manner.
This structure is fully illustrated by the following woodcuts and descriptions. These
sketches could have been greatly multiplied, but these only have been selected from a nu-
merous collection, particularly in the higher rocks. w
Jointed Structure of the Limestones.
The direction of these joints in the limestone is for the most part very uniformſ; still, how-
ever, there are exceptions. Where the rock is exposed upon the surface, these lines of joints
are very manifest, and from weathering, often present wide fissures; these, in favorable situa-
tions, become so much worn beneath the surface as to be cavernous. They influence the
thin soil upon the surface by draining the water into the fissures of the rock, often leaving the
surface dry. • - - - -
In the lower part of the Niagara limestone these are prominent characters, and in the quar-
ries near Lockport, are of the greatest importance in facilitating the removal of the stone.
The central portion of the mass, which is concretionary and irregularly bedded, does not
present the well-defined joints of the lower part; indeed, in some places they appear to be
nearly or entirely wanting. Again in the upper part, which is thinly bedded, though curved
and apparently contorted, the joints are strongly defined, and together with the thinly bedded
structure, enable the workmen to quarry the rock without the aid of blasting. The sketch
on page 94 is a natural face of the rock in the direction of a joint.
In the limestones of the Helderberg division, this structure is more strongly manifested than
in the Niagara limestone. The joints on the surface often appear as broad fissures, leading
to caverns below, and the sinkholes observed are produced by the widening of these fissures.
Where this rock is wrought for quarry stone, the same structure is strongly manifested, the
lines of division often penetrating the entire rock. The woodcut below is an illustration of a
quarry worked on the line of outcrop, and shows the facility offered in removing the rock.
JOINTED STRUCTURE. 303
*
Limestone quarry near Waterloo.
In the impure limestones of the Salt group, these joints are often manifested in some degree
of perfection, but they are more usually closed, and evident on the surface only from weather-
ing. They are much more numerous than in the purer calcareous rocks, and separate the
A
layers into small blocks. - - - - *- --
Jointed Structure of the Shales and Sandstones.
In the incoherent strata of soft shales, like the Niagara shale and those of the Onondaga
salt group, as well as in some of the softer shales of the higher groups, the jointed structure
is but very imperfectly developed. In the softer portions of the salt group, this structure is
scarcely more developed than in the recent clays; and almost the same may be said of the
soft red marl and shale of the Medina sandstone, and the shale of the Niagara group. In
some parts of the Hamilton group, and in the Cashaqua shale of the Portage group, joints
are often scarcely perceptible. In the impure and less compact sandstones, the joints are
imperfectly developed; but in the purer and more compact strata of this nature, they are very
perfect. In all parts of the higher groups, however, the joints are very perfectly developed,
and very clearly and exactly defined. In the slaty shales, where they have been freshly
exposed, the surfaces are scarcely separated, and of the most perfect smoothness and regu-
larity. The surfaces are usually plane, but sometimes they are curved, as in the following
woodcuts: - - - : - -
\, * . J
GEOLOGY OF THE FOURTH DISTRICT.
º:
;:
É=
£:=
3:2::
à
à
à
|
|
#:#
4:
É
§s
ſº- º
º:
º: § -->
§§º --
§§ º
Tº-º-º-º-º-º:
Fig. 1, is a sketch from the western shore of Seneca lake, near Big-stream point.
Fig. 2, is a sketch from the bank of the creek above Lodi falls, near Wyckoff's mill.
a, a, a, are uniform planes of perfect smoothness. -
b, b, are curved surfaces, having a general vertical direction, and of equal smoothness with the others.
}
r
Sometimes the interstratified impure sandstones interrupt the joint, and the lines above and
below do not coincide. In the greater number of instances, however, these thin strata offer
no impediment to the passage of the joint, and the whole mass is divided into huge blocks
Or prisms. This structure, particularly along the lake shores, presents some of the most
picturesque scenery, resembling the gigantic ruins of Cyclopean architecture, crowned in its
decay by trees, shrubs and festoons of moss and vines. - .
The following sketch is from a beautiful example of this kind, on the shore of Cayuga lake,
~,
near Ogden's ferry.
JOINTED STRUCTURE. 305
The cliffs are divided by vertical and curving joints, separating a long line into blocks of
ten to twenty feet long and broad. The action of the water is constantly widening these
joints, and undermining the masses. These fall down, one after the other, and their fragments
are dispersed by the waters; sometimes a single one of a whole range is left standing alone,
with a long interval between it and any other, as in the illustration below (fig. 1). In fig. 2,
the high block is isolated from the cliff behind it, and from the range to which it belongs on
the left. Its relations to the adjoining cliff may be seen by the range of concretions which
are thickly dispersed through a certain stratum. Some of these concretions are divided by
the joint as regularly as if sawn asunder; in other instances they project from the mass,
having been unaffected by this divisional structure. - *
150.
The process by which these masses are destroyed, by the undermining action of the waves
below and the weathering from above, is illustrated in the following woodcut:
[Geol. 4th Dist.] 39
306 - GEOLOGY OF THE FOURTH DISTRICT.
The strata are composed of alternating hard and soft materials, which unequally resist the
influence of water and air. After a time the wearing action of the water below is so great
that the base becomes too narrow to sustain the mass above, and it usually falls over on the
seaward side, when it is soon dashed in pieces, and is removed by the waves.
The “Chimney rock,” below Jefferson, about two miles from the head of Seneca lake,
is another example of this kind. A single block, originally one of a range separated by
vertical planes, remains standing against the cliff, like a huge chimney upon the outside of a
wall, to which it bears a fancied resemblance. *.
The following is a sketch of this place:
3: E º->
23 *-º:
2 :==#EE-> ~-
º: :=#Ess
3. #=SS
Where the water finds its way entirely around, the mass wears down much sooner than
where one side continues attached to the main cliff. In some instances these blocks stand
out along the line of the cliff in bold relief; and, from long weathering and wearing by the
waves, have become rounded in outline, and the point of their attachment is constantly nar-
rowed, until finally a separation takes place. The projecting edge overhangs the lake by
several feet, and the water is so soon drained off through the smaller fissures that the larger
trees near the edge die. - .
F==== ºº: --
#== §s. ºś
É --> -ss
- º £º: *-
E-T / Sº == Fºsº; ºCº's -
========>===ºs-e- Fºssºs::$ 3's #E
=== ==E= º ====tº:=-tº-sº =º?:3S= º g-
==2-#3 5:S:===s-º-º: - s:==rezz:=#==####$sºÉ
:=>== -----. 㺠- Yºº-ji=E: -- - ...-- -, T-ºv --- - Sºse: šáž:::::::::::::
=========?: =#EE::=E-ºº-ºº::=====E=: ##s=#:
- =-- - --> tº: ===º:Sºº-º-º: -------> ºr :s---> :::::::::$3.
-º-º-º- º :-º-º: -- ---, >:--> -- :=º-º: -: --> :
- ::::::::::::::: : 3:#º:- . =º.--> - 3:3:25: *-*
£ºś=<====-->======º 3: s:
########::::::::::=##$35: =~~---->== †ºº --- 3:S
===#: º:-- -------. --- - º >. --
--- E-22. - :=s====--> - -* =-sº
* É=3=ºs:::::::::35:5:=> → - -2
--- ##########=< Iº * =
*>==- :=> =-: 3:#E :
- º-
ãº:
JOINTED STRUCTURE. . 307
In many places, it is evident that there has been but little change during long periods; for
large trees are found growing in the fissures, and others upon the separated blocks, extending
their roots down the sides of these and into the soil below. Such appearances are observable
in the banks of deep ravines, where there is conclusive evidence that large streams of water
have flowed at some former period. ~ . .
Jointed Structure of the Conglomerate.
This structure in the conglomerate usually divides the blocks into more rectangular forms
than the rocks below. In the outliers of this rock which appear in the southern counties, the
whole mass often appears in isolated blocks, as can be seen in the illustration under the
description of that rock. The following sketch also illustrates the same. In the corner of
the block, on the left, it will be seen that a portion has been removed by the intersection of
two planes, which did not extend entirely to the surface. -
154.
º:=: -.
*:E::=> *-*
*-*- ==E-E . F.
.:- EE c. E.
-- --- -- -—Es--" -—---sº
* -- * -- . =:E- º---------º
====== ~e:=:...t= —
===========
- -- - :====---------
--- rºººº-ººt:- == ---
----- ºÉº ===zº º #==== --_
T-Eº º ift ====
º º º - ==E ---
- fº-ºº:
#º º iſ: - ºùù Ž%hº
##### T- #j}% ====
& sº 3:= rº ºft||| | - - % ſº =–5-> - -
sº sº - -—Jiří lill E=
º sº." ājº ſº — sº-> & illiºn T- T-ºff -
#ºiſi | º -> iſ H==
ºuillº,
| riff
#
}
Rºllſ
308 GEOLOGY OF THE FOURTH DISTRICT.
CHAPTER x.
Mineral and Gas Springs rising from the Rocks of the New-York System in the
Fourth District. -
The general phenomena of springs have been noticed under each rock or group, where
there existed any circumstances to modify their production, or otherwise affect their fre-
quency or copiousness. The origin of all the springs of pure water, or that of ordinary
purity, is simple and readily understood ; in other instances, there seems more obscurity
attendant upon them. - - - -
In this district the only mineral springs of interest are the salines, the sulphur springs, the
inflammable gas springs, and the springs of Canoga, yielding nitrogen.
1. NITRogBN SPRINGs.
The only springs in the district which are known to yield nitrogen, are at Canoga in Seneca
county. One only is very copious, and, therefore, the only one usually noticed. It is situ-
ated at the base of a gentle slope, and near the southern termination of the Corniferous
limestone. The basin is not over six feet in diameter, but the water rises, in less quantity,
over a space of twenty feet. The sand and gravel are kept in continual agitation, rising in
little cones, and again falling away and appearing at another point. The water, in its ascent,
is accompanied by nitrogen gas, which rises to the surface in large quantities. The force of
the water and the escape of the gas give the spring the appearance of a boiling vat. The
water is perfectly limpid, and leaves no sediment of any kind; it first spreads over a bottom
of gravel and boulders, from which the finer parts have been removed for several rods, and
then flows quietly through a narrow channel towards the lake. The outlet of this spring is
joined by a similar smaller one, which flows in from the northeast. There are also several
points in a swamp near this, where the same gas issues.
These springs have all the characters, except temperature, of the thermal springs along the
eastern border of the State, the gas from which is known to be chiefly nitrogen. The springs
of Canoga, with several in Franklin county, N. Y., are the only ones I have seen yielding
nitrogen, which were not above the ordinary temperature of the place. The temperature
of these springs is about 40°, Fahrenheit's scale. -
MINERAL AND GASEOUS SPRINGs. - 309
From the facts before noticed, under the description of Corniferous limestone, there is
scarcely a doubt but these springs have their origin along a line of fault or fracture in the
strata. Those on the eastern side of the Cayuga lake at Springport have, probably, the same
origin; and it is interesting to observe that those in the eastern part of New-York are in simi-
lar situations, but much nearer to strata of igneous or hypogene origin. I am also informed by
Mr. Vanuxem, that many which he has examined in Virginia, and at the south, are in similar
situations.” Those of Chateaugay are near the junction of the granite and Potsdam sandstone,
and in the Calciferous sandrock. . . . -
2. SPRINGs Evolving CARBURETTED HYDROGEN AND PETROLEUM (Burning Springs).
Springs of this character are numerous in the Fourth District. Sometimes the gas alone
is the only product; and in others it is accompanied by petroleum, or liquid bitumen, which
spreads over the surface of the water, and can be collected in considerable quantities. These
are the “burning springs,” which in our younger days were such a marvel as a part of
geographical knowledge. . - ~s. - --
These springs are chiefly confined to the higher rocks, though there are a few places where
they occur in the lower beds. The lowest situation in the Fourth District is at Gasport in
Niagara county: this has already been noticed in the description of the Medina sandstone.
Along the outlet of Crooked lake, there are several places where this gas is seen to rise
from the canal, and streams of water. The principal point is where there is an undulation
in the strata. - - . -
A mile south of the village of Rushville, in Yates county, there are one or two springs
which emit a considerable quantity of this gas ; and when ignited, it continues to burn as it
rises to the surface of the water. It was formerly conducted to a house near by, and used
for lighting and warming the apartments. It is a popular belief, that wherever this gas rises,
coal exists beneath the surface; and accordingly an excavation was commenced at this place,
which of course resulted in disappointment. The geological situation is in shales of the
Portage group. - - - -
In the town of Bristol, Ontario county, there are several springs from which this gas issues.
The quantity is often large, and might be turned to some economical purpose. -
The “Oil spring,” as it is termed, is situated on the dividing line of Allegany and Catta-
raugus counties. “It is a dirty circular pool, about eighteen feet in diameter, filled nearly
to its margin with foul water, having, at the time we saw it, a small quantity of petroleum in
clots floating upon its surface.”f - - - -
This description of the famed oil spring corresponds with its appearance when subsequently
visited. There was a small quantity of the gas issuing at intervals through the viscid film
- • Q - $ - -
* Prof. W. B. Rogers has since published an elaborate paper on the “Connection of Thermal Springs in Virginia with
Axes and Faults.” (Transactions of the Association of American Geologists and Naturalists.)
+ VANUxEM, Annual Report of 1837.
310 GEOLOGY OF THE FOURTH DISTRICT.
which covered its surface. About half a pint of the petroleum, or Seneca oil, was collected.
This spring is at the base of a hill on the Reservation, of one mile square, belonging to the
Cattaraugus Indians, who reside on the Allegany river.
There are several other places in the county of less importance, where both petroleum an
carburetted hydrogen gas are evolved from springs. The rocks, in nearly all localities, emit
a bituminous odor on percussion, and the fluid bitumen often exudes from pores or cavities.
In Cattaraugus county, carburetted hydrogen gas issues from the springs and running
streams in numerous places. In the town of Freedom, there is an oil spring similar in many
respects to that of Cuba in Allegany county. The spring is situated on a slope below the
outcropping edge of a highly bituminous sandstone, which rests on an impervious shale, as
seen in the woodcut.
a. The position of the spring.
The origin of this spring is doubtless from the bituminous matter which is carried down by
the water as it percolates through the interstices of the sandstone. Several excavations have
been made near this spring for coal; and in one of these, after breaking through a hard stra-
tum in the shale, a large quantity of the petroleum, mixed with water, rushed up, entirely
filling the cavity. The quantity was so great, that for a long time several gallons were daily
collected. - - - -
In Chautauque county, a larger quantity of the gas issues from springs, streams and pools,
than elsewhere in the district. In many instances the gas is accompanied by petroleum, which
forms a thin pellicle upon the surface of the water; in other places the gas rises alone, and
sometimes the petroleum occurs where there is no visible evolution of the gas.
Near Forrestville, there is a copious emission of this gas; and it has been in contemplation
to convey it to the village, for the purpose of lighting the houses and stores. At Laona there
is a stratum of highly bituminous sandstone, and the water, rising to the surface, is accom-
panied by petroleum and gas. The sandstone appears to be charged with this fluid : it issues
from the pores on fresh fracture; and specimens, after remaining for two years in the cabinet,
still emit a strong bituminous odor. -
MINERAL AND GASEOUS SPRINGS. 3II
The village of Fredonia is lighted with this gas, which issues from fissures in the shale
forming the bed of the stream at this place. During the day, it is collected in a reservoir,
and furnishes sufficient for purposes required. -
At Portland harbor, the Light-house is illuminated with this gas, supplied from the margin
of a small stream on the lake shore, half a mile northeast of the harbor. The quantity at this
place is so great that no reservoir is required ; and I was informed, that during the night, as
much passed off by the “escape pipe” as was consumed.
Large quantities of this gas issue from the waters of the lake near the shore, for three miles
northeast of Portland harbor, and in numerous other places farther north and east. At Buf-
fington's well," it is constantly rising from the lake near the shore, apparently sufficient in the
space of a few rods to illuminate a city. This product will doubtless be turned to important
account when the population shall increase, and villages be formed in the vicinity. It could
even at the present time be used in the village of Portland harbor, and with small expense
conducted to Westfield. The only requisite expense will be the fixtures for collecting and
purifying: the supply is constant, and probably inexhaustible. -
This gas doubtless issues from the earth in equal quantities in other places, but they cannot
be readily detected except on the presence of water. Along the sheltered banks of the lake,
the odor of the gas is constantly perceptible for miles, and its presence is thus manifest when
the water is too rough to render its escape perceptible.
Numerous other localities of minor importance might be noticed, but the foregoing are
sufficient, as its existence and uses are well known.
3. SULPHURETTED HYDROGEN SPRINGs.
These springs are numerous, and occur in almost every rock in the district; but those which
are copious in water, and highly charged with gas, are confined to few situations. The most
important springs are those issuing from the rocks of the upper part of the Onondaga salt
group; these being almost the only ones resorted to for the medicinal properties of their waters.
They contain, besides the gas, carbonate and sulphate of lime, which are deposited upon the
stones and twigs over which the water flows. At some there is a considerable formation of
calcareous tufa, often covered with a yellow coating, which apparently consists of sulphur and
sulphate of lime. The water is usually perfectly limpid, though sometimes it has a whitish
or chalky appearance when first flowing from the spring.
Springs of this nature which issue from different rocks, have an aspect and general character
which indicate their relative geological positions. In the shales of the Niagara group, the
water has usually a dark appearance in the spring, though limpid, and differs essentially from
those of the Salt group; while those in the higher rocks are not only less copious, but are
* This is a deep boring (642 feet), made in search of salt water, on the supposition that if the level of tide water was reached,
the salt water would be found. This is not the only similar ignis fatuus which has been followed in searching for coal, salt water
and the precious metals; neither have these visionary projects ended at the present time.
312 - GEOLOGY OF THE FOURTH DISTRICT.
often marked by a black and red deposit, as well as sometimes a whitish stain upon the rock
or in the bottom of the spring. The flow of water is feeble, and it is less strongly impregnated
with gas. - - -
Such being the fact in relation to these springs, we are to look for some general cause why
those in the Onondaga salt group are so much more copious, and strongly charged with gas,
than any others. Since also there is no general line of disturbance or uplifting along the
outcropping edge of this group, we cannot attribute their origin to any source below the rock
itself; for if so, they would as probably be in other situations a little farther north or south;
but as the facts stand, it is upon the very margin of this formation where they occur. The
jointed and fissured limestone above affords a passage for the water from the surface, which
falls down upon the impure argillaceous limestones beneath, and passes through these to an
impervious stratum, when it rises to the surface.
Now all we have to account for, is the source of the gas, and by what process the water
becomes thus charged? The rock contains iron pyrites, often very intimately blended; and
on burning in the kiln, a large quantity of pure sulphur sublimes, and lodges upon the stones
about the top. It is impossible, perhaps, to say that this is in a pure state in the rock; but
may it not probably be in some other combination than with iron, and one which may be more
readily decomposed by water and atmospheric agents Since sulphur is known to be diffused
through this rock, either in a free or combined state, it is very rational to suppose that it
enters into combination with the hydrogen of the water, and thus produces the phenomena
of gas springs. - -
The decomposition of sulphuret of iron, in moderately damp situations, gives origin to
sulphate of iron; but this could not exist in the water of these springs, though there is usually
present some other sulphates, as the sulphate of lime or of magnesia. In the higher shales,
which all contain iron pyrites, we find the decomposition leaving an iron stain, and often
sulphate of iron, almost always sulphate of alumina, and always sulphate of lime, which
forms in small crystals upon the slaty laminæ. These products are the results of the decom-
position of iron pyrites, in districts and situations where they are exposed to the weathering
influences, but where there is not sufficient water to form springs. They do not differ, so far
as they go, from those of sulphuretted hydrogen springs. I have made no detailed examina-
tion, but there is little doubt but an analysis of these dry efflorescences would prove them to
contain all the products of sulphur springs, or at least to bear an equal comparison to the
products of one spring with another. During rains, the odor of this gas is perceived from
the situations where these dry efflorescences appear, though not at other times. -
On the Niagara river, a short distance above Lewiston, there is a copious spring issuing
from the cliff, highly charged with sulphuretted hydrogen gas, and the water impregnated with
sulphate of magnesia; and judging from some incrustations upon the stone, it contains both
the sulphate and carbonate of lime. Now this spring has its origin in a highly magnesian
limestone, which is also charged with iron pyrites. In sheltered situations under the cliff,
this rock is rapidly decomposed, and produces sulphate of magnesia, with a little sulphate of
iron and carbonate and sulphate of lime. These substances can be obtained to the amount of
MINERAL AND GASEOUS SPRINGs. 3H3
several pounds in the space of a few feet. The decomposition of this rock, beyond ordinary
exposure, from the percolation of water from above, will produce precisely the materials with
which the spring is charged; and there can remain no reasonable doubt of this being their
origin generally, or even universally in the Fourth District. - T
The quantity of this gas is not surprising, when we reflect that a single ounce of the bi-
sulphuret of iron, if decomposed and its sulphur united with hydrogen, will produce more
than two hundred cubic inches of the gas. This is a large amount of this noxious vapor from
so small a quantity of the material; the decomposition of a few pounds of pyrites will be
sufficient to supply an ordinary sulphur spring for several months; and in the more copious
springs, it must be recollected that there are large surfaces exposed to the action of air and
Water. -
The increased temperature noticed in all these springs may be due to chemical decomposi-
tion and recomposition, so that more caloric is evolved from the solids formed than is required
for the production of the gas. Their great uniformity of temperature in widely different
positions, would indicate the cause to be in chemical action, rather than to proceed from any
deep-seated and general source, as we may suppose is the case with the thermal springs
which evolve only nitrogen. - - -
The same views will apply to those springs evolving carburetted hydrogen; the most co-
pious being in the highly bituminous shales of the Portage and Chemung groups, while it is
produced in smaller quantities from the lower rocks. Its origin is thus satisfactorily proved,
and we have the same evidences regarding the production of the hydrosulphuretted springs.
In the same rocks in the eastern part of the State, which at the west give origin to the car-
buretted hydrogen and petroleum, that substance is not manifest, and there are no springs of
the kind. Again, the rocks most productive of the hydrosulphuretted springs are equally
charged with sulphuret of iron in the eastern part of the State, and give origin to as copious
and strongly charged waters as at the west. -
It is true that in some places carburetted hydrogen is very abundant at points where there
has been a slight disturbance or uplifting of the strata; but it appears to be in consequence of
finding more rapid egress through the numerous joints, rather than in any manner to depend
on such fracture for its origin; and in many of the most copious ones, no such marks of
disturbance are visible. -
On September 1st, 1841, the temperature of the Avon springs was 50° Fahrenheit; the
lower one a fraction less. The upper spring discharges about eight or ten gallons per minute;
the lower one, fifty-four gallons per minute. - - * :
The temperature of the several springs at Manchester, which are the most copious of any
in the district, and from which a larger quantity of gas is evolved than in any other, is 50°
and 519 of Fahrenheit's scale. The quantity of water is much greater than at Avon.
The situation of the Avon springs is illustrated by the following woodcut:
[Geol. 4th DIST.] 40
314 - GEOLOGY OF THE FOURTH DISTRICT.
156.
1. Limestone of the Onofidaga salt group. a. Upper spring.
2. Onondaga and Corniferous limestones. b. Lower spring.
3. Marcellus shale. -
The upper spring rises near the junction of the Onondaga salt group and the Corniferous
limestone. The source, however, is much deeper, as it can be penetrated with a rod to the
depth of fifteen feet or more. The lower spring rises from the same strata, at a lower posi-
tion. There are also in the same neighborhood, at about the same level as the lower spring,
several others in which the water is strongly impregnated with gas.
The position of the springs at Manchester, in Ontario county, is precisely similar.
1. Limestone of the Onondaga salt group. a. Point at which the springs issue.
2. Onondaga and Corniferous limestones. -
3. Marcellus shale.
The shale above the limestone does not approach within a mile or more of the edge of that
rock; and it can scarcely be supposed to give origin, by the decomposition of its iron pyrites,
to the gas which rises from the rock below." - º
4. SALINEs, or BRINE SPRINGs.
The principal brine springs of the Fourth District have been noticed under the head of
Medina sandstone and the Onondaga salt group. The first have their origin in the red shales
and marls of the Medina sandstone, extending throughout the whole length of the district, and
likewise known in Canada in the same rock. In the early settlement of the country, salt was
manufactured from these springs; but its quality was often inferior, and highly colored from
the red marl. The brine is also very impure, from the presence of the chlorides of calcium
and magnesium. - - - -
Since the supply of brine in Onondaga county is so much more copious, and the facility of
manufactnring and transporting the salt so much increased, all these springs in the Medina
—sº
* The large proportion of iron pyrites in the Marcellus shale, has been supposed by some to give origin to this gas.
MINERAL AND GASEOUS SPRINGS,
315
|
sandstone have fallen into disuse, though very recently there seems some prospect of the
manufacture being renewed. The situations, in most instances, are unfavorable to large
accumulations of water upon the surface, and boring has not been attended with the most
satisfactory results. So long as salt can be manufactured at the present prices, there is little
probability that these springs will be of any importance.
There are several unimportant brine springs in the higher rocks. The most remarkable of
these is at York in Livingston county, which, for some time after its discovery, yielded a large
supply of water, but which has diminished since that time. Prof. Dewey informs me that the
the water gives evidence of a large proportion of iodine, on the application of the usual tests.
The only brine spring of importance in the Onondaga salt group, is in Elba, Genesee
county, and has already been described.
CATALOGUE of the principal Min
eral Springs in the Fourth District, with their geological
position and products. -
Gas evolved.
Particular locality.
Kind of spring. Geological position. Contained mineral County.
- substances.
Brine------- Marls of the Medina. A few bubbles of carb. Chloride of sodium, Monroe ----- Penfield, a mile from Lake Ontario, on the
sandstone, hydrogen, - land of Mr. Greig.
Brine------- Medina sandstone-...] ----. - - - - - - - - - - - - - - - 1 - - - - - - - - - - - - - - - - - - Monroe ----- Near the head of Irondequoit bay.
Brine------- Medina sandstone---|--------------------|------------------ Monroe -----| Town of Greece, 9 miles N.W. of Rochester.
Brine-------| Medina sandstone---|--------------------|------------------ Monroe ----- Three springs, or the banks of Salmon creek,
- - town of Clarkson. ... "
Brine------- Medina sandstone---! -------------------|------------------ Monroe ----- Town of Clarkson, 6 miles north of the pre- ||
- - - ceding, on land of Mr. Baxter. |s
Brine------- Medina sandstone---| Carbonic acid ------- Chlor, of sodium, &c, Wayne ----- Near the head of Little Sodus bay.
Brine------- Onondaga salt group. -------------------- Chloride of sodium, Wayne -----| Two miles east of Lockville.
Brine------- Marls of Onondaga Carbonic acid -------| Chlor. of sod, cal] Wayne -----| Town of Galen, Old Galen salt spring.
salt group, - * mag., sulph, and -
t carb. lime, }:
Brine------- Marls of Onondaga Carburetted hydrogen| Chloride of sodium, Wayne ----- Village of Clyde, boring to the depth of 200
salt group, and carbonic acid, - feet.
Brine------- Marls of Onondaga| Carburetted hydrogen, Chlor, of sodium, &c. Wayne -----| Two miles east of Clyde.
salt group, - -
Brine------- Miſſ *istone... gº ºs º ºs º ºs º ºs º we as m = * * * * * s = Chlor. of sod., mag- Wayne -----| Banks of creek north of Wolcott furnace.
nesium and iron, -
Brine------- Medina sandstone---|-------------------- Chloride of sodium, Orleans ----| Fairhaven, in the town of Gaines. |
Brine------- Medina sandstone---|-------------------- Chloride of sodium, Orleans ----| Town of Kendall, lot 137. Salt was formerly |
- made at this spring. -
Brine------- Medina sandstone---|-------------------- Ditto ---------- Orleans ----| Near Scofield's mill, on Johnson's creek, in ||
- - t the town of Yates. . . |:
Brime------- Medina sandstone---! -------------------- Ditto ---------- Orleans ----| Town of Murray near Sandy creek. Two
- other similar springs in the same town.
Brine------- Medina sandstone---|-------------------- Ditto ---------- Orleans ----| Medina, Oak-orchard creek.
Brine------- Medina sandstone---! -------------------- Ditto ---------- Niagara.----- Three miles north of Lockport.
Brine-------| Medina sandstone---|-------------------- Ditto ---------- Niagara.----. Several on Eighteen-mile creek.
Brine------- Medina sandstone---! -------------------- Ditto ---------- Niagara.----- Several on Johnson's and Golden-hill creeks.
Brine------- Shale of Hamilton| -------------------- Ditto ---------- Livingston --| York, near Hall's saw mill.
Chalybeate--
Chalybeate--
Chalybeate--
Sulphureous,
group,
Portage group
Onondaga salt group,
Onondaga salt group,
Chemung group-----
Chemung group-----
Medina sandstone---
Portage group
Onondaga salt group.
Portage group ------
Sulphureous,
Portage group
sº m ºn an º' tº sº se tº sº we s is is ºn “” ºn sm was as
• * * * * * * * * * * * * * * * * = = s.
- - - - - - - - - - - - - - - - - - - -
we me - * * * * * * * * * * * - - tº me ºn tº
* * * * *
Sulphuretted hydrogen
Sulphuretted hydrogen
* = ± = - - - as ºs º- - - - º ºs - - -
Sulphate of lime---
Steuben ----
Genesee ----
Genesee ----
Cattaraugus -
Steuben ----
Niagara.-----
Steuben ---.
Cattaraugust
Cattaraugus:
Near the village of Jefferson. |
Town of Elba, cight miles N.W. of Batavia. }
Town of Elba, land of John G. Satterlee.
Near Rutledge, several unimportant ones.
La Grange, land of Mr. Davis. |:
Two miles north of Lewiston, on land of Capt.
Leonard. ---
Near Jefferson, head of Seneca lake.
| Williamsville, land of Mr. Youngs.
Town of Randolph.
Several on the banks of Cattaraugus creek.
40*
316
GEOLOGY OF THE FOURTH DISTRICT.
(CATALOGUE CONCLUDED.)
oxide of iron,
º
Kind of spring. Geological position. Gas evolved. Contained mineral County. Particular locality.
substances. *
Sulphureous, Portage group ------ Sulphuretted hydrogen Sulphate of lime---| Chautauque -| One mile east of Van Buren harbor.
| Sulphureous, Portage group ------ Sulphuretted hydrogen| Ditto ---------- Chautauque -| Near the village of Laona.
Sulphureous, Portage group ------| Ditto ------------ Ditto ---------- Chautauque - Several in and near the village of Fredonia.
Sulphureous, Onondaga salt group, Ditto ------------|------------------ Erie --------| Grand island.
Sulphureous, Hamilton group----- Ditto ------------|------------------ Erie-------- Several on the Indian reservation east of Buf-
* falo.
Sulphureous, Onondaga salt group, Ditto ------------|------------------ Erie-------- Several in the towns of Amherst and Clarence,
below the limestone terrace.
Sulphureous, Onondaga salt group, Ditto' ------------|------------------ Genesee ----| Several in Byron and Bergen.
Sulphureous, Onondaga salt group, Ditto ------------|------------------ Livingston ...| Caledonia village. -
upper part, * . . - .
Sulphureous, Onondaga salt group, Ditto ------------ Sulphate of lime, Livingston --| Several near West Avon, strongly impregnated.
. magnesia and soda, . -
Sulphureous, Hamilton group----- Pitto ------------|-- ---------------- Livingston --| Near Moscow.
Sulphureous, Niagara group ------ Pitto ------------|------------------ Monroe ----- Village of Ogden,
Sulphureous, Niagara group ------ Pitto ------------|------------------ Monroe -----| Longmuir's in the city of Rochester.
Sulphureous, Niagara group -----. Pitto ------------|------------------ Monroe ----- Monroe spring, five miles east of Rochester.
Sulphureous, Niagara and Ononda-| Ditto ------------|------------------ Monroe -----| Several in the towns of Mendon and Pittsford.
- ga salt groups, ** -
Sulphureous, Niagara group ------ Pitto ------------|------------------ Monroe -----| Ogden, on the land of Timothy Colby.
Sulphureous, Clinton group ------ Pitto ------------|------------------ Orleans ----- Holley village ; two ; weak. .
Sulphureous, Niagara group ------ Pitto ------------|------------------ Niagara----- Several near Lockport; one three miles south.
Sulphureous, Onondaga salt group, Ditto ------------|------------------ Niagara.----- o Tonawanda creek, two miles from the vil-
- age. -
Sulphureous, Niagara group ------ Pitto ------------|------------------ Niagara-...---| Bank of the river two miles below the falls.
Sulphureous, Onondaga salt group, Pitto ------------|------------------ Niagara.----- Pendleton. * *
Sulphureous, Niagara group ------ Pitto ------------|------------------ Niagara.-----| Three miles east of Lewiston.
Sulphureous, Onondaga salt group, Pitto ------------ Sulphate and carbo- Ontario ----- Clifton springs, town of Manchester; several
. nate of lime, - very copious and highly impregnated.
Sulphureous, Onondaga salt group, Ditto ------------|------------------ Ontario -----| Banks of the outlet of Canandaigua lake.
Sulphureous, Cormif limestone --| Ditto ------------|------------------ Seneca -----| Waterloo.
Sulphureous, Chemung group-----| Ditto ------------|------------------ Steuben ----| Campbelltown. e
Sulphureous, Chemung group----- Ditto ------------|------------------ Steuben ----| Near the post office in Jasper.
Sulphureous, Chemung group-----| Ditto ------------|------------------| Steuben ----| Town of Canisteo.
Sulphureous, Portage group ------ Ditto ------------|------------------ Steuben ----| Urbana. .
Sulphureous, Onondaga salt group, Ditto ------------|------------------ Wayne -----| Brown's millpond, south of Newark.
Sulphureous, Medina sandstone ... Ditto ------------|------------------| Wayne -----| On Salmon creek, near the forge in Sodus.
Sulphureous, Onondaga salt group, Ditto ------------|------------------ Wayne -----| At and near Palmyra. -
Sulphureous, Onondaga salt group. Ditto ------------|------------------ Wayne ----- Village of Clyde. &
Sulphureous, Niagara group ----- - Ditto ------------|------------------ Wayne -----| Half a mile northeast Marion Centre.
Inflamm, gas, Portage group ------ Carburetted hydrogen, ------------------ Chautauque - In and near the village of Fredonia.
Inflamm. gas, Portage group ------ Carburetted hydrogen, ------------------ Chautauque - Van Buren harbor.
Inflamm. gas, Portage group ------ Ditto ------------|------------------ Chautauque - Buffington's well,
Inflamm. gas, Portage group ------ Ditto ------------|------------------ Chautauque - Portland harbor.
Inflamm, gas, Chemung group----- Ditto ------------|------------------ Chautauque - Town of Sheridan.
Inflamm, gas, Chemung group-----| Ditto ------------|------------------ Cattaraugus - ol spring of Fredom, and several other loca-
- 1tleS. -
Inflamm, gas, Niagara group ------| Ditto ------------|------------------ Monroe -----| Town of Riga,
Inflamm. gas, Medina sandstone---| Ditto ------------|------------------| Monroe ----- Near the mouth of Genesee river.
Inflamm. gas, Medina sandstone---| Ditto ------------ ------------------| Niagara ----| Gasport, six miles east of Lockport.
Inflamm. gas, Medina sandstone---| Ditto ------------|------------------ Niagara ----| Several places between Lockport and Middle-
- - - port on the canal,
Inflamm. gas, Genesee slate ------ Ditto ------------|------------------ Ontario -----| Bristol hollow, town of Bristol.
Inflamm. gas, Hamilton group----- Ditto ------------|------------------ Ontario ----- East Bloomfield and Richmond.
Inflamm, gas, Hamilton group-----| Ditto ------------|------------------ Ontario -----| On both sides of the Canandaigua lake, within
three miles of the village.
Inflamm. gas, Portage group -----. Ditto ------------|------------------ Yates ------ Federal hollow, one mile from Rushville.
Nitrogen ----| Cornif limestone ---|--------------------|------------------ Seneca -----| Canoga springs, mear the village of Canoga.
Sulphuric Onondaga salt group, --------------------| Sulphuric acid, with Genesee ----| Towns of Byron and Bergen.
acid, lime, alumina and
NEW RED SANDSTONE, AND TERTIARY. 317
CHAPTER XI.
NEW RED SANDSTONE, AND TERTIARY.
Of the formations (enumerated in the tabular view, pages 17 to 19) which succeed the
Carboniferous system, there is nothing in the Fourth District which belongs to the period of
the New Red Sandstone. The only known development of this rock in the State is in the
southeastern part, within the limits of the First District. - -
The Tertiary formation is principally embraced within the First and Second Districts,
though the clays and sands extending along the valley of Lake Ontario are nowise distinguish-
able in their lithological aspect from those which contain organic remains in the valleys of
St. Lawrence and Champlain. From a comparison of these deposits, there is no difference
which would justify a reference to different epochs; and it seems indeed quite probable that
they are of the same age, and the products of a period subsequent to the gravel by which they
are in many places underlaid, though in others the clay rests upon the rocky strata, which
apparently remained uncovered after the deposition of the gravel. But if the presence of
organic remains is to be the test in distinguishing the Tertiary from other superficial deposits,
then all the blue and yellow clays, succeeded by yellow sands, in the Fourth District, must
be referred to the subsequent period of drift. 's - -
During the summer of 1836, I examined the fossiliferous deposits on the Salmon river, a
few miles from the St. Lawrence, and found them resting upon the Calciferous sandrock, which
bears evidence of what is termed diluvial or glacio-aqueous action in the numerous striae and
grooves upon its surface. The lower deposit of shells, principally Sanguinolaria, rests upon a
fine gravel. Dr. Emmons has shown the same fact with regard to this formation on Lake
Champlain. Thus it appears that in reference to the lower formations, those of Ontario,
St. Lawrence and Champlain valleys hold the same relative position; but since the former
contain no shells, they will be described in this report among the superficial deposits, without
reference to the Tertiary period. - -
I have remarked, that no organic remains have been found in these clays or sands on Lake
Ontario. I am not unaware, however, that fragments of wood, freshwater shells, etc. are said
to be discovered; but in all cases which have come under my own observation, these are of
subsequent periods, either covered by a slide of the older materials, or enclosed in a superficial
deposit. Although more time might have been given to these formations, yet those of more
immediate interest have absorbed the principal share of my attention.
3.18 GEOLOGY OF THE FOURTH DISTRICT.
\
CHAPTER XII.
SUPERFICIAL DETRITUS.
The superficial materials covering the surface of the older stratified rocks of the Fourth
District, and to a great extent concealing them from view, are due to successive operations on
a more or less extended scale, which have broken up the indurated strata, and worn the frag-
ments to different degrees of comminution. The agencies producing these effects have been
sometimes almost universal throughout the extent of this district, and at others confined within
very limited areas; and we may trace them through successive stages from the simple opera-
tions of freezing water, the running of streams and rivers, the washing of waves upon the
lake shores, through more stupendous exhibitions, as the damming up of river channels, the
excavation of new ones, the bursting of lakes, etc., till the phenomena pass beyond our means
of comparison, and leave us to conjecture in what manner these have resulted, as they trans-
cend the usual effects of causes before our eyes. These more extensive and least known
operations have produced those deposits of loose materials, sometimes called diluvium; but
as this term includes many deposits of local or very modern origin, the term drift has been
proposed, as being unobjectionable in this respect, and unambiguous in its meaning.”
The scoring and striating of the surface of the strata, which seems to have been effected at
the same period, as well as the excavation of broad and deep river channels, and the like, are
all referred to an agency concerning which there is yet no settled opinion. The plausible
theories of one observer are modified or overturned by new facts, or the bolder speculations of
another; and at this moment, even the most extravagant hypotheses are advanced in order to
account for these familiar phenomena. - - * ~ *
While so many conflicting hypotheses are thus before the public, it would be of little mo-
ment to advocate the one or the other; and therefore the facts observed in the Fourth District
will be stated, with the unavoidable conclusions to which they lead. There is always, in
these investigations, great need of caution, not to confound the products or the phenomena of
two or more periods; for it can readily be demonstrated that the superficial deposits of the
State are of different ages, sometimes distinct and separate, and again mingled and confused.
No one theory of formation can account for the whole, and we are therefore often to seek for
causes close at hand, rather than venture too far into conjecture.f -
* See Murchison's Silurian Researches, page 509, note.
f Mr. Murchison has very clearly shown the successive periods in which the superficial accumulations of certain parts of
England and Wales were produced; and the facts observed in New-York correspond precisely with his views and observations,
supeRFICIAL DETRITUS. - 319
All the northern part of the district, and the low slopes and deeper valleys of the southern
part, are covered to a greater or less depth by superficial materials of more northern origin,
mingled with those of the rock on which the deposit rests.
The extreme northern margin consists of the worn fragments of lower stratified rocks, as
the Hudson river group, intermingled with a large proportion of those of the Medina sand-
stone. The former gradually diminish as we progress southward, and are finally lost alto-
gether; those of the different successive formations taking their place, and constituting, in
turn, either the greater or smaller part of the whole accumulation. Those which are of the
most durable character continue farthest, and they may even be traced as far as the Penn-
sylvania line; but, in their passage southward, they have been much worn, and greatly dimi-
nished in size. Still, by careful examination, traces of all the stratified rocks on the north
may be met with in these depositions. - -
As we pass southward, however, over the successive formations, we find that all have suf-
fered greatly from denudation, and that the abraded fragments of each constititute a large
proportion of the superficial materials resting on its southern neighbor. The size of the
fragments always bears a proportion to the distance they have been transported from the
parent rock; and in the Fourth Distriºt we often find a huge mass of a northern rock resting
upon the margin of the one next south of it, while at a distance of ten or twenty miles farther
south, only small pebbles of the same occur. -
These remarks apply to the older deposits; and while it sometimes happens that a huge
fragment has been transported many miles southward, having suffered little attrition, it
seems due to some operation subsequent to that of the great accumulation below. Even in
the deep valleys at the southern margin of the State, may be found pebbles of all the northern
rocks of the district, except the soft shales, which will not withstand the transportation. *
We find resting upon the limestone and calcareous shale formations a dark colored gravel,
ranging from fine to coarse. This has accumulated most in sheltered situations where a
succeeding bed or stratum rises to the south of it, as if it had been pushed onward over the
bottom, lodging against the projecting edges of the strata. In this way it often happens that
a rock, in its more northern extension, is covered with sand or clay, while the coarser mate-
rials are pushed farther onward. These phenomena occur where the deposit is evenly distri-
buted over the surface; in other places the coarser and finer materials, intermingled in the
greatest confusion, are heaped up into conical hills, which are thickly scattered over the sur-
face. Again, the same materials are accumulated in long hills or ridges, having a determi-
nate direction, and sloping down from a high northern elevation to the general level of the
country on the south. - -
The Driſt or Boulder period, the products of which are often confounded with more ancient deposits of similar materials, is cer-
tainly the most recent of all, and, except where they are intermingled with the previous deposits, are always the most superficial.
In the valley of the Hudson, in the vicinity of Albany and Troy, I have searched in vain for a boulder or pebble of granite, or of
any rock older than the Potsdam sandstone, in the deposits below the clay; while in a period subsequent to the deposition of the
clays and sands, boulders of granite are by no means rare. - - -
It may be remarked here, that the old deposits alluded to contain abundance of quartz pebbles, and quartz with green chlorite;
but these are from the quartz veins in the partially altered rocks of the age of the Hudson river group.
320 GEOLOGY OF THE FOURTH DISTRICT.
This condition of the surface clearly indicates the condition of the waters from which this
deposition was made. On the one hand we have comparatively an evenly distributed deposit,
as if made by the retiring waters of an ocean; in another, the long hills, with certain direc- -
tions, show a determinate course and more powerful current in the ocean, while the irregular
conical and dome-shaped hills, with deep, bowl-shaped cavities, show the force of contend-
ing currents, or of other obstructions in the course of the transported materials.
It becomes very evident, therefore, that to whatever cause we choose to attribute the pheno-
mena of the superficial detritus of the Fourth District, the whole surface has been permanently
covered by water; for it seems impossible that partial inundations could have produced the
uniform character and disposition of the materials which we find spread over the surface, not
only of the limited area we have been describing, but over several hundred miles farther east
and west. That partial influences have operated, and partial inundations taken place, there
is no doubt; and some of their effects will be enumerated. It is very possible also that many
of the varying features of this deposit are due to causes not now recognized, and less universal
than at first view may be supposed. In these I would often be disposed to include the abrupt,
conical and elongated ridges, which, with no determinate direction, often cover considerable
spaces, when the surrounding country is comparatively level.
There is also another fact to be borne in mind, viz. that the materials of the hypogene or
primary rocks constitute but a comparatively small proportion of the superficial accumula-
tions of Western New-York. The great bulk of the deposit, whether evenly distributed or
irregularly raised into hills and ridges, is, nevertheless, composed, in large proportion, of the
rock but a short distance on the north, or perhaps of the one on which it rests, with a con-
stantly decreasing proportion of rocks of northern origin. It is true that boulders of granite
and gneiss are often scattered in great profusion over the surface, sometimes indeed to the
almost entire exclusion of every other rock, and they are more or less numerous in almost all
situations where the superficial detritus has accumulated; still they rarely enter into the
great mass so as to constitute any large proportion of the whole. -
Although it may not be impossible that some of these boulders, of granite and other rocks
of similar nature, have been transported at the period of this great accumulation of local drift,
and forming a part of the great moving mass; yet they are, for the most part, due to sub-
sequent operations; brought thither by a force which has transported them alone, and which
has had no great effect, even upon the previously deposited superficial detritus; and we must
carefully guard against confounding these accumulations with those of antecedent formation.
In many instances there has been an intermingling of the products of two periods, and
sometimes the granite boulders appear to have rolled down from higher elevations, often in-
deed resting upon the most recent superficial deposits." Instances of this kind are visible along
the valleys of the northern part of the district. On the broad northern slope towards Lake
Ontario, where hills are distant, there are numerous and extensive fields of boulders, resting
upon the surface, or but partially imbedded in the soil, and holding such a position that it is
* Such as river alluvium, et :,
suPERFICIAL DETRITUs. 3.21
quite evident they are of subsequent origin to the great body of detritus. We find similar
exhibitions too upon the great western prairies, where, for many miles, the difference in eleva-
tion is not more than fifty feet; and here we observe long lines of boulders stretching away
for miles beyond the reach of vision, as if once forming a line of coast, or deposited along
some channel or course of a current, though the general surface indicates no influence upon
this portion beyond what is common to the whole. -
The causes which have given origin to the superficial accumulations, will be noticed under
different heads. The most universal and uniform in character were evidently produced be-
neath the water of the ocean, or during the elevation of this portion of country." -
The immense amount of denudation which has taken place in this portion of the State, could
only have been accomplished beneath the ocean, when it entirely covered the surface of the
country, and was subject to tides and currents like the present oceans. This view, too, ac- -
quires additional support from the fact, that portions of country along the sea shore, which
have been recently elevated above the water, bear a very close resemblance in many particu-
lars to the more anciently denuded and elevated districts. Along the Massachusetts bay,
where the high hills of loose materials contain shells of recent marine species, leaving no
doubt of their modern origin, the surface has all the characters of those sections in western
New-York covered by drift or diluvium. Extensive tracts often occur, which are almost
unbroken; while again the surface is broken into irregular hills or ridges, with deep bowl-
shaped depressions, or long valleys, which often communicate in more extensive ones, or
are enclosed on all sides by drift. The character of large tracts farther south, along the
Atlantic coast, is extremely similar; and when we consider the difference in the nature of the
strata beneath, and the influence of a longer period of weathering, the analogy becomes very
striking. Thus we may conceive this whole extent of country to have been submerged be-
neath the ocean for a long period; and that in its subsequent elevation it has been washed by
the advancing and retiring waves, which have worn the deep indentations in the limestone
cliffs, and broken up the northern edges of the strata.
Notwithstanding, however, that this operation would explain many of the phenomena pre-
sented, still there are others which it would leave unexplained. In those portions of the sea
coast which I have had an opportunity of examining, the inlets and indentations are always
broad towards the ocean, and narrowing as they recede. In many of our older valleys, how-
ever, we perceive a different form; the sides are nearly parallel for miles in extent, and they
do not present the broad or trumpet-shaped mouths which are common to the coast inlets, or
^.
those in the face of our limestone terraces.
The valleys of Seneca, Cayuga and Crooked lakes, Canandaigua lake and others, are of
nearly equal width from one extremity to the other, with nearly perpendicular banks above the
water. It seems hardly possible that such channels could be excavated by the advancing and
retiring waves, upon a coast which was gradually emerging from beneath an ocean.
* This cause has been explained by Mr. Hayes, in an article published in the American Journal of Science, Wol. 35, No. 1.
[GEOL. 4th DIST.] 41
322 GEOLOGY OF THE FOURTH DISTRICT.
No theory of this kind, moreover, seems sufficient to account for the grooved and striated
surfaces of the rocks in place, which hold a uniform direction, and which occur in all situa-
tions, and upon the highest and lowest points, In all situations which have been observed
beyond the influence of deep valleys, these scorings or striae have a uniform direction, or
varying but a few degrees from N.N.E. and S.S.W.
The local origin of nearly all, and perhaps all the ancient drift of the district under con-
sideration, can be shown by an examination of numerous sections upon the lake shore, in the
river courses, and in artificial excavations which reach to the rocky strata. These sections,
where made in situations beyond the reach of modern disturbing causes, show very clearly
the conditions under which the superficial detritus has accumulated. The action of the pre-
sent ocean upon cliffs and beds of rock extending beneath its surface, is nowhere more clearly
represented than in the sections of detritus resting upon the stratified rocks of western New-
York. - - - -
The shores of Lake Ontario offer some of the most instructive exhibitions of this kind, and
indeed it might almost be considered a continuous section from one extremity of the district
to the other. The following section on the east side of Irondequoit bay, illustrates in a perfect
manner the general character of these superficial deposits. -
158. .
2.É.
㺠'º.
** gº § - âşa * 2: sº & -- sºsºs
㺠E. Şää jºššč sºft#s
& gºš ºf JºšSS Š šāºš
- - ... * *** *. > -- * '*'. ‘e, 2–– •. & 7
· · · =.. --SS - - - - ----- * w
gº * —rºſ. TN Tº"--
ESNERNºNNNSN •
º §§§ 'Nº - Nº N- .*-*.*.* SN 6
.* * & - .
wº • SS *. A * * * * * S. : N • * . Wr." NYS".. & . -
se wº : To - • . • *. . . - - - - - - - *º * * e. " & sº
Ç * SSZCºzzº,
Section at Vinton's quarry, Irondequoit bay.
7. The soil of sandy loam.
6. A coarse deposit of pebbles of the Medina sandstone below, with gravel and sand.
5. Stratum of pebbles and sand. -
4. Stratum of sandstone pebbles, cemented into a conglomerate by oxide of iron and carbonate of lime.
3. Bed of fine sand. - - -
2. Fragments and rolled masses of the sandstone below, with gravel and sand. This contains a few pebbles of the
shaly, calcareous sandstone next on the north. -
1. Medina sandstone. Shaly, with bands of green.
Numerous similar sections, varying in some unimportant details, might be given, all showing
that the older deposit resting upon the red sandstone is composed of fragments of that rock,
more or less worn, with a small admixture of other materials. This red gravel of the lower
deposit is always to be relied on, as indicating the immediate proximity of the sandstone. The
a'
SUPERFICIAL DETRITUS, 323
following section, about seventy miles farther west, illustrates the same position, though the
conditions seem not to have been as equal throughout as in the first. • ?
159.
sº •r --
º a tº SA 2 & Ś
º Š
§§ § § SN §§
º
*:
*-
*,
wº-
A.
it.
A.
rt " , , . ~~ * r * = rºw
* ----' -- . ~ - . . .
~.
** *
*
*s - r -- *|†º.
Section of the bank of Lake Ontario, town of Wilson, Niagara county.
4. The soil of clayey loam, with clay below.
3. Gravel, clay and sand, of the neighboring rocks, folding over and passing beneath No. 2.
2. Blue clay and gravel. The pebbles are principally of the rocks of the Hudson river group.
1. Red clay and gravel of the Medina sandstone.
The clay deposit of the surface is often succeeded by sand and sandy loam, as in Monroe
county; and this sometimes rests upon the gravel, without the intervention of clay.
In most instances, there is evidence of the most perfect uniformity in the production of these
deposits; and when they can be traced over so large an area, it is plain that the few apparent
exceptions will be met by some other explanation. As before remarked, where these ac-
cumulations form hills and ridges, they do not always preserve the same regularity as in the
widely distributed and more shallow deposits. This may have resulted, in some instances,
from subsequent causes, or from the force of contending currents while the ocean covered the
surface. In many instances, the sand is irregularly deposited; and at others, there appear
to have been partial depositions and denudations during the period of its formation.
The following is a sketch by the late Dr. G. W. Boyd, of a hill about two miles east of
Rochester. The ridge has been excavated in an east and west direction, for the passage of a
road, presenting a depth of thirty feet or more.
-- --~~~~ ===
- - crºssº
--- 77 strº-ººººººººº.
ºśº
- * *
Nº Mººs wº 0. CŞ
- tº ar," e. ea tºº.º. A "&
es 3::$º **** º AR5 t
Sººſ, , A. t \****
Nº. sº: `et
&º Žº
- -- ſº E-
º &
3 - 4.
1 & 2. Deposits of fine sand variously inclined, with a few layers of gravel.
3. Coarse gravel, with large boulders of limestone.
4. A subsequent deposit of sand, like Nos. 1 and 2.
33,
41*
324 GEOLOGY OF THE FOURTH DISTRICT.
There appear to have been several periods of deposition, where the laminae do not coincide,
and which are separated by stronger lines of division. The section is a perfect representation
of the face of the hill: nearly all the strata dip towards the west, and the accumulation doubt-
less took place from this direction, from the heaping of the coarse gravel upon the fine sand.
The gravel consists principally of waterworn fragments of the Niagara limestone, on which
the whole deposit rests, and of the sandstones and limestones on the north. There are some
boulders of the limestone, from two to four feet in diameter, worn perfectly smooth, or often
striated with shallow grooves; and from the fact that this is the subjacent rock, they have
received their rounded forms and smooth surfaces from attrition near the spot where we now
find them. -> l
This character of the hills of the northern range of counties could be illustrated by nu-
merous sections, showing the diagonal lamination, removal and re-deposition of deposits.
Scarcely a hill can be excavated, where this kind of structure is not observed in a greater or
less degree, and sometimes the whole deposit is in such confusion as to present no definable
structure.
In the southern counties, after leaving the deeper valleys, the superficial detritus is less,
and differs in character from that in some of the more northern parts of the district. Its con-
nection with the stratified rocks below is the same, and resting upon them we find an ac-
cumulation of fragments of variable dimensions, mixed with clay, gravel and rounded pebbles.
The materials, however, bear less evidence of attrition than those farther north, and there are
but few rounded pebbles. The “flat gravel” of the hills, and the “round gravel” of the deep
valleys, has before been noticed. These terms serve to distinguish different degrees of attri-
tion, as well as marking different portions of country. The origin of the mass is the same as
in the northern part of the district, but it has been less subjected to subsequent operations, and
may be regarded as presenting the primitive state of drift, or diluvium. It must be recollected
also that in all these situations there are no primary boulders intermingled with the mass,
though they are occasionally seen upon the surface. The materials of the northern stratified
rocks of the district appear never to have been lifted to this elevated portion of the country,
and are found only in the lower valleys. * .
I may here remark, that these investigations were commenced with a belief in certain views
and theories regarding the production of drift; but as my observations progressed, the diff-
culty of reconciling the facts with these preconceived notions became constantly more apparent. -
In conclusion, therefore, although some of the foregoing arguments may not appear quite
satisfactory, or free from doubt, it must be remembered that long continued and extensive
examinations are necessary to put us in possession of all the facts bearing upon the subject,
while comparatively little time could be devoted to this department; and I have been unable
to revisit localities, where, two, three, and even four years ago I noted circumstances, and
appearances, which at present, with the different views to which I have been led by multiplied
observations, coincide with and confirm these inferences. - -
The theory usually inculcated in regard to the great body of drift covering the surface of
the strata, is that it consists of granite and other materials of far northern origin, which have
SUPERFICIAL DETRITUS. - 325
been moved forward over the surface with resistless force, and, in their passage, uplifting,
breaking and transporting the fragments of strata over which they pass. That blocks of
granite, either enclosed in ice or moved by other means, have been the principal agents in
effecting diluvial phenomena; that they have scored and grooved the rocks in their passage,
and breaking up the strata, and mingling themselves with the mass, have been driven onward,
carrying everything before them in one general mêlée. That such may have been the case
in some instances, or in limited localities, cannot be denied ; but that it ever has been over
any great extent of country, will scarcely admit of proof." -
A glimpse of a more rational explanation has occasionally offered itself, and after an exami-
nation of my notes, and the numerous sections made on the spot, I have found, almost univer-
sally, that they correspond with the preceding sections and their explanation, viz. a bed of
broken fragments, with worn pebbles resting upon the rock from which they are derived.
The granite and other materials of a far northern origin rarely constitute a part; and I am
not prepared to say that, in any instance where they do form a part, the deposit has not under-
gone some subsequent change. -
If we adopt the views indicated by the facts here presented, it does not preclude the proba-
bility of deposits of purely northern origin (containing rocks of granite, gneiss, etc.) from
resting directly upon any other stratified rock; for even allowing the earliest drift to have
been formed by the wearing of the ocean and the breaking up of the strata by the action of
waves, still all this may have been subsequently removed, and another deposit have taken its
place. Such, doubtless, has often happened; and if a previous deposit is removed to make
room for another, then we should naturally expect, in many instances, a mingling of the two.
* >
Grooved, striated and polished frocks.
Intimately connected with the subject of the older drift is that of grooves, or striae upon the
surface of strata which lie immediately beneath. All the rocks of the Fourth District which
are of a sufficient hardness to receive and retain such impressions, and which have since with-
stood the action of the weather, are more or less marked in this manner. From the Medina
sandstone, at the level of Lake Ontario, to the summit of the conglomerate of the Carbonife-
rous system, some of the strata in every group bear upon their surfaces these markings of
former abrasion and the evidence of moving force. These, too, for the most part, bear a very
uniform and decided direction, varying but a few degrees from N. 35° E. and S. 35° W. in
their general course. Short and shallow striae are abundant, which vary ten and fifteen de-
grees from this direction; but these have no continuous course, and apparently fall into the
main direction after a few feet.
* In primary regions there are no other rocks than granite, gneiss and their associates; and consequently whatever may be the
age, or by whatever means produced, the superficial deposits are charged with these masses.
326 GEOLOGY OF THE FOURTH DISTRICT.
These markings range from the slightest possible scratch to grooves of half an inch in
width, and from one-eighth to one-fourth of an inch in depth. Such grooves could only have
been made by some hard substance, moved with great force, and under great pressure, over
the surface of the strata; for not only do we see the deep grooves and shallow striae, but
fragments are broken out as we approach a fissure in the stratum, as if crushed by some heavy
body. Such phenomena, which are frequently witnessed, are illustrated in the following
woodcut, where the lower side of the specimen, as shown in the cut, is broken off obliquely,
so that the upper surface recedes six inches beyond the lower. This took place upon the
southern edge of a mass at the crossing of a fissure. The mode of fracture indicates an im-
mense weight, pressed upon the surface, but not a quick, heavy blow. The grooves follow,
somewhat obliquely, the fractured slope, which was probably made near the close of the ope
ration; for, in many instances, such surfaces are afterwards polished, but this one retains its
freshness. There are in this specimen (and the same often occurs in others) two sets of
striae; one, being the prevailing direction, is as stated above, while the other is very nearly
north and south. f - -
161.
Sº §§ RN º §N
§§
§§§N
YW. N W
§
sº
W
W
N º,
§ W
º NYMº
§ º Nº. º
º . . . . º. º.º.º.º.
Grooved and polished limestone, Lockport.
The outcropping edges of strata, previously polished and grooved, are often overturned
upon the rock, in place, by this force moving southward. Upon the surface from which the
above specimen was selected, I have seen frequent examples of this kind; and in some in-
stances the fragment is partially rounded, possessing the character of a boulder. At this
locality the grooves are often large and deep, while in other places they are fine, and the sur-
face is nearly polished. The materials resting above this rock are fine sand and sometimes
clay; but in no place in the same neigborhood have I seen gravel, and only occasionally large
fragments of the rock itself from the outcropping edges. A few miles farther south, however,
there is a great accumulation of gravel, covering the strata.
SUPERFICIAL DETRITUS. 327
At Rochester, on the other hand, the surface of the limestone is finely striated, and almost
perfectly polished, by this abrading action. So evenly is the surface worn, that I have taken
slabs a foot square, and laying the faces in contact, there is no perceptible difference in the
planes. The material here resting upon the rock is fine sandy loam ; and in another locality,
a mile farther south, it is covered by coarse gravel of limestone and sandstone pebbles, with
boulders of granite. These slabs are, for the most part, too smooth to be illustrated in an
engraving, but can readily be understood from comparison to a partially polished slab of
marble. - - - - -
The surface of the Niagara limestone, which is covered with drift materials, is from two
to seven miles wide, and extends the whole length of the district. In all localities where this
rock has been exposed, I have observed these striae, in greater or less perfection, but in no
other place so fine, or with the surfaces so evenly polished, as at Rochester. The example
of this rock alone, shows how universal has been the operation of this agent.” -
The great force and powerful abrasive action is well illustrated in the accompanying plate,
which is from a specimen obtained at Black-Rock, from the surface of the Corniferous lime-
stone, and is completely covered with these grooves and striae. It presents some interesting
phenomena, from the presence of little nodular concretions of hornstone, which, in some
places, stand out from the general surface, having, from their harder nature, evidently acted
as a barrier to the abrading force; and there is a long, elevated ridge of the stone upon the
southern side of these, which was thus protected, as a pebble or a fixed stone in a running
stream allows the accumulation of sand or mud beyond it. In one or two examples these
nodules of hornstone have been broken off, and fracturing below the surface, have left a de-
pression, which is partially smoothed out in the same manner as the surface. There cannot
be a more instructive exhibition of this abrading force than is here presented, where the
different degrees of hardness in the two substances have fully illustrated their respective
power in resisting the force applied. The surface, when free from these nodules, is not a
perfect plane, but appears in broad undulations, with the elevations and depressions parallel
to the striae, and produced by the wearing of the surface. In this instance the direction of the
grooves, with scarcely a single exception, is N. 35° E. and S. 35° W.f
On the banks of the Niagara river, and also at Lockport and elsewhere, I have, in some
instances, found the direction of these grooves variable, though having the same general
course. At Lockport, however, I was informed by Mr. Barrett, that after clearing the earth
from the rock, previous to excavating the Erie canal, one large groove was noticed, which
was measured, and found to extend, without the least variation, more than one hundred feet.
It will be remarked that the direction of these grooves corresponds very nearly with the
direction of the great excavating force, and the deep valleys of the lakes and rivers of the
*I find in my notes the direction of the grooves at Rochester marked as N.N.E. and S.S.W. with some slight variations.
#See a communication on the subject of these grooved and polished surfaces, by George E. Hayes and R. W. Haskin, in
the American Journal of Science.
328 GEOLOGY OF THE FOURTH DISTRICT.
*
western part of the State. Whether these are to be referred to the same origin, or as having
been produced at the same period; or if the striae only followed the previous direction of the
valleys, may be a question not easily decided. I shall, however, show that in some instances,
at least, they are connected with the excavation of large masses of the rocky strata.
The shore of Lake Erie, from Buffalo to the Pennsylvania line, in a southwesterly direction,
coincides very nearly with the dip of the strata, presenting many interesting sections, as il-
lustrated in Plates W. and VI. The rocky strata in vertical cliffs are succeeded by deposits
of gravel, clay and loam ; the lowest, as before remarked, consisting of fragments of the
subjacent strata, but little worn, and intermingled with clay and gravel. Along this extensive
line of natural section, there are some interesting exhibitions of the connection of these de-
posits of such widely distant geological epochs. - -
Sometimes the projecting edge of a stratum is uplifted, and the gravel and fragments pressed
beneath it, elevating and sometimes overturning its edge, and loosening others some distance
beyond. In this way, I have seen a stratum fractured and elevated at an angle of 30 or 45
degrees, imbedded in the drift which was pressed on from the northward. Stupendous opera-
tions of this kind have sometimes taken place, and immense masses of the strata have been
elevated and moved forwards. The section, Plate VIII., is a correct representation of the cliff
of Lake Erie, in Portland, Chautauque county, as it appeared in October, 1840. The section
is explained upon the plate. The two upper strata are of the ordinary character of the deep
loam and clayey gravel deposits along the lake shore. The rocky strata below have been
uplifted, broken and contorted; the fragments intermingled with clay and gravel, and the same
pressed beneath the strata, which otherwise appear to be in place. At some points the strata
are completely broken up, and the fragments separated; in other places, they are simply
shattered, without being otherwise much disturbed. In such cases they appear as if they had
been subjected to violent oscillation, like ice when the water is agitated by wind; they are
broken into short fragments, as seen in the whole of the central part of the section. Be-
tween e and f, the clay, gravel and fragments are folded and contorted, as if violently pressed
forward from the north. It appears as if the whole mass above the shelf 1, 2, 3, had been
uplifted and moved onward by some powerful force, which at the same time pressed the
finer materials into all the interstices. - -
In several places where the strata are slightly separated, and the spaces filled with frag-
ments, the surfaces are scored and striated precisely in the manner before described. It seems
impossible that any other agent than what is here perceptible should have had access to these
places, or aided in producing the result. The broken fragments insinuated between the layers,
and the movement of the whole upper portion with its load of gravel and clay, seems sufficient
to have produced the phenomena in question; and if in this case such causes are adequate to
these results, why may not the same, under other conditions, produce the like, or more
extended effects? The efficiency of the force cannot be doubted. In this instance, it only
requires that a longer continued operation should have broken up the whole of these liſted
strata, to have left a tolerably even surface, scored and striated like all the strata surfaces
SUPERFICIAL DETRITUS. -- 329
described. It requires simply the insinuation of sand and pebbles between the layers, and then
that the upper one be made to move over the lower, to produce all the observed phenomena.
In the softer shales, where the striae are sometimes preserved, they are deeper than in the
limestones and other hard rocks. In the black shale about Dunkirk harbor, all the grooves
are broad and deep, compared with those of Black-Rock or Niagara, and there seems no other
cause except the soft character of the shale. .--
There is a remarkable fact connected with these striated surfaces, which may be noticed
here. The terrace at Lewiston is formed by the upper part of the Medina sandstone, the
Clinton group, and the Niagara shale, capped by about twenty feet of limestone as already
described. The following section illustrates the succession : -
162,
1, 2 & 3. Medina sandstone. 4. Clinton group. 5. Shale of Niagara group. 6. Limestone of Niagara group.
The top of this terrace is three hundred and fifty feet above Lake Ontario, and more than
two hundred feet above the plain about Lewiston. The projecting shelf of rock a, is the
limestone of the Clinton group, about one hundred feet below the top of the Terrace. The
surface of this projecting mass is deeply grooved and striated, the grooves having a general
southern tendency, but more irregular than where they are seen upon the limestone on the
top of the terrace; and at this place, the surfaces two hundred feet lower and one hundred
feet higher are scored in like manner. We naturally inquire, what agency could produce
this effect? Here is an abrupt elevation of one hundred feet above the striated surface; and
it seems hardly possible that an island of ice, loaded with granite boulders, could have stranded
upon this projecting shelf, and produced the scoring, and that at the same time others above.
and below could be made in like manner. .
It may perhaps not be out of place here to consider a few facts connected with these striated
and polished surfaces, in their relation to the theories of glacial and glacio-aqueous action, as
the agencies in producing such phenomena, and others connected with superficial deposits.
It will be borne in mind that the Fourth District, in its greatest elevation of about two thousand
feet above tide water, descends to the level of Lake Ontario, two hundred and forty feet above
tide, for the most part in a series of steps or terraces over the successive formations; the
[GEoL. 4th DIST.] 42
330 GEOLOGY OF THE FOURTH DISTRICT,
surfaces of these, from the highest to the lowest, are grooved and striated, and in the lime-
stones often beautifully polished. - - ... "
In the first place, we are unacquainted with any high land on the north, from which glaciers
could originate to cover this entire surface. The relative levels, as well as the directions of
the water courses, must also have been different, to have allowed of such effects from glaciers;
for under present circumstances, we should hardly expect to find a glacier advancing from
the valley of Lake Ontario, toward the southern margin of the State, and ascending nearly
two thousand feet in one hundred miles. Even admitting the theory to be true, it is probable
that the glaciers would originate among the mountains of Canada, or farther north among the
primary rocks; and in this event, we might expect to meet intermingled with the earliest drift a
considerable proportion of granite, and other pebbles and boulders of the older rocks, which is
not the case. There is also another circumstance connected with glacial action, which deserves
inquiry. The deep valleys were either excavated previously; at that period; or subsequently.
If these were excavated previously, then the power which accomplished it was sufficient to
produce all the striae and grooves which we now find. It can hardly be supposed that these
excavations were made at the time the glaciers were progressing southward; for no such
power is attributed to them, and they usually follow the course of valleys previously formed.
If we attribute these valleys to subsequent causes, then we have a power capable of obliterating
all traces of glacial action. -
Not being familiar with the views of M. Agassiz from his own writings, I may have an
imperfect or erroneous opinion of his theory; but so far as I understand it, it seems inadequate
to produce all the phenomena in question, and inapplicable to this portion of the country.
In regard to glacio-aqueous action, there are other considerations to be taken into view.
Glaciers, loaded with fragments of rock, may have drifted from the base of mountains, and
in passing over shallow portions of the ocean, have scored the surfaces of the strata; but in
order to accomplish this, a peculiar condition of things is necessary. It requires that the
surface be free from the accumulation of detritus, which in the ocean cannot be, except the
elevated rocks; and we can never find any portion of country which has been for a con-
siderable time submerged beneath the ocean, but is covered to a greater or less depth with
superficial detritus. Again, it requires that the surface should be even; or that there should
be an immense number of these bergs at all conceivable depths, to touch the varying elevation
of the strata. And even under the most favorable circumstances, it requires that thousands
and millions should have traversed the ocean, and stranded upon the bottom, in order to pro-
duce the wearing down, the polishing, and the myriads of small and large grooves and striae
which mark the surface of strata. - -
It is not pretended that. more than a few masses of granite or other rocks can be attached
to the bottom of an ice island, and therefore but few points could touch the bottom at one time;
and if we reflect that they may often be as irregular and jagged in their outline beneath the
surface as they are above it, then the points will be few indeed. If an ice island were to
be stranded in the valley of Lake Ontario, supposing the whole country covered with water,
it would require to be elevated three hundred feet to groove the Niagara limestone, and one
suPERFICIAL DETRITUS. 331
hundred more to touch the surface of the next limestone above, and so on to the end of the
series. This objection, however, can be met by supposing the country gradually rising from
the water, and that the highest parts were first scored, and the lower ones afterwards. But
if we take this view, we then make the admission that the great inequalities of the country
were previously existing; and if these were made, we want no farther power to furnish the
explanation we seek; for the same power which excavated a deep valley in a determinate
direction, if more diffused in its operation, may have grooved and polished the strata over wide
8.Téa S. - t -
The countless numbers of inconceivably fine striae upon the surfaces of the limestones, many
of which are only visible by a magnifier, seem a strong objection to the theory that these
phenomena have been produced by ice floes; and this fact of itself seems to me conclusive
testimony against it. The lower surfaces of these icebergs are confessedly very irregular, and
from the falling down of portions from above, the equilibrium is often destroyed, and the mass
turns partially or entirely upside down. The fine striae and polished surfaces are more like
what is produced when one even surface is moved over another, having sand or gravel be-
tween the two; indeed, not very unlike the preliminary polishing of marble when the motion
is all in one direction. It seems impossible that a mass of ice, with fragments of rock set in
it, could have pressed so closely as to have produced such an effect.
The polishing and striating of surfaces of limestone and other rocks, no harder than the
sandstones of the Fourth District, is, after all, no process which requires such tremendous
force as is sometimes called into action; though if great force be applied, it would, doubtless,
break up the strata, and still leave a striated surface below.” - ..
Another objection to this view is in the oblique furrows, which often diverge from the regu-
lar course. Had all these been produced by fragments, like gravers, fixed in a mass of ice,
no such furrows could have been made ; and if we maintain that these were worn by loose
masses on the surface, which were moved by contact with the ice, then they are as capable
of making the same impressions if moved by any other force.
There is also another fact worthy of notice, which is that the vertical faces of joints, when
much separated and nearly coinciding with the direction of these grooves, are polished or
striated, in the same manner as the surfaces. Hundreds of instances can be observed near
the outcropping edges of the Niagara limestone; but this is readily understood by any one
who has observed the chinks and fissures in harder rocks along the sea shore, which are
similarly polished by the washing in of sand and pebbles by the advancing and retiring waves.
sº-
* I have seen a quarry at Lockport, the entrance to which was along the surface of a stratum in the direction of the dip;
the superior strata had been removed, and this surface left in its natural state. After drawing stone from the quarry, on the
- common stone-drag, for a few weeks, the surface of the stratum became worn smooth and striated, and in some places nearly
polished. This was done merely by the fragments ground between the wood of the drag and the stratum below, as it
moved over the surface. In this instance, there were few fragments or pebbles of any other rock than the limestone,
42*
332 GEOLOGY OF THE FOURTH DISTRICT.
CHAPTER XIII.
Position and mode of transport of the great northern boulders.
The general contour of the surface of the Fourth District has been already described, and
the limits of the successive terraces and plateaux are not more perfectly defined than is the
distribution of granite boulders, particularly in the northern part. That portion occupied by
the Medina sandstone, and forming the first plateau above Lake Ontario, is often plentifully
covered with boulders. These usually lie upon the surface, and always upon the previously
described deposits of drift. They are not evenly distributed, but often appear in immense
numbers, scattered over several acres; while beyond this, for a greater distance, few are to
be found. There appears to be no law regulating their distribution, though they are more
abundant in the eastern than in the western part of the district. -
In passing along the Ridge road from Wayne county to the Niagara river, these boulders
may often be seen in immense numbers on the low ground just north of the ridge, as if they
had been brought there while the water was limited by this barrier, and spread over the bot-
tom in shallow water near the shore. - -
In higher situations, and just beneath the great limestone terrace, they again appear in
abundance, as if this elevation prevented their farther advance to the south. Standing upon
this high plateau and looking over the low ground on the north, the position of these boulder-
fields can be distinctly traced. They are thickly scattered over spaces varying from a quarter
of an acre to two or three acres, and sometimes even more ; and these spots are separated
from half a mile to two or three miles, with only a few stray ones between.
The broad plateau formed by the surface of the Niagara limestone and the Onondaga salt
group, is sometimes thickly strewed by boulders of granite. The most abundant fields are
in Wayne, and the eastern part of Monroe county; and going westward from the Genesee,
they are less so, becoming extremely rare in Erie and Niagara counties. They occur here in -
the same manner as before described. -
As we ascend the second limestone terrace, formed by the Helderberg range of limestones
extending westward, boulders become perceptibly less numerous; they are irregularly scat-
tered, and at few points present the thickly covered fields which we observe a few miles far-
ther north. Very few ascend the slope formed by the passage of the Hamilton group to the
rocks above; and in all the previous cases, they seem to have been brought on at intervals in
great numbers, and their limits bounded by the different elevations of the surface.
NORTHERN BOULDERs. 333
As we pass southwards over the higher groups, boulders become exceedingly rare; and
finally toward the southern margin of the State, they are rarely seen. - - -
This approach to the southern limits of these northern masses corresponds with what is
observed throughout the whole west, as far as the Mississippi. The drift containing northern
boulders of granite is scarcely observable in the southern part of Ohio and Indiana; and I am
informed by Mr. Lawrence, of Aurora, Ia, who has travelled much in that part of the country
on both sides of the Ohio, that the valley of this river seems to be a limit to the northern
boulders, and they rarely (if ever) appear upon the south of it. Such facts are of the highest
interest, as enabling us to arrive at important conclusions regarding the means of transport of
those huge blocks, which, over the whole continent, and even over the whole world, seem, at
certain periods, to have poured down from the north in such immense numbers. Wherever
any attention has been given to their southern extension, it has always been found confined
within certain parallels, and we have no authentic account of northern boulders in intertropical
regions.” -- - - ,-
The condition of the boulders in the Fourth District, is the same generally with these
masses over every part of the country where they have been noticed. Some of them bear
evidence of much wearing, being actually striated upon the surface, and sometimes flattened
on one side, as if held in that position while moved over a bottom of gravel or sand resting
upon the strata beneath.f For the most part, however, they bear no evidence of attrition be-
yond what similar masses do a few miles from their parent rock, and thus offer no argument
for their mode of transportation. I have met with many which are very angular, and with no
appearance of attrition beyond what the weathering in their present situations would produce.f
Even if these boulders were all rounded, it furnishes no argument that they were worn into
this form during their transportation from their original beds to places where we now find them.
The process by which fragments of granite become rounded boulders, is illustrated by the
desquamation which takes place in some granites, the weathering in place, and the attrition
in mountain streams soon after leaving their native beds. In the mountainous region of
* In Virginia and North-Carolina, I have seen rounded masses of hard granite and greenstone lying upon the surface, and
having much the appearance of boulders. In every case where I examined these, I found them to consist of masses which had
become rounded from weathering in place, and were fragments of beds or veins of a hard rock in a surrounding softer mass which
had disintegrated. Prof. Rogers says he has ſound pebbles of granite in Tennessee. -
# I attach very little importance to the supposition that boulders of granite have been worn smooth and striated upon one side
while fixed in a floating mass of ice, and in that way worm down while rubbing over a stony bottom. Some boulders of this kind,
which I have seen, are less than a foot in thickness, and two feet in length. Now is it possible that such a boulder, having
rounded edges, can be fixed in a mass of ice, so as to allow of such force being applied to it, without falling out, unless the pres-
sure were constant? The beds of many of the streams in the granite regions of New-York are literally paved with boulders,
which remain fixed in certain positions, while any fresh accumulation of stones and earth, with ice and water, pass over them,
rendering the upper sides very smooth, while the lower may be little worn. Cam such occurrences offer any explanation of this.
apparent polishing on one side by transportation? - -
† There is a mass of greenstone in the town of Riga, Monroe county, which bears no marks of having been broken artificially,
the angles of which are as perfect and unworn as a fragment just precipitated from a mass of the rock in place. On the road to
Nunda, south of Mount Morris, there is a similar fragment of greenstone, which weighs several tons, and still the angles are very
little worn. Numerous other examples might be cited, offering the same evidence as these. -
334 - GEOLOGY OF THE FOURTH DISTRICT.
Northern New-York, I have seen examples where a slide or avalanche of snow and ice has
brought down from a mountain side an immense number of fragments of the dark felspathic
granite, freshly torn from the rock in place. These are precipitated into a narrow gorge,
or the channel of a stream; succeeding floods bring down other fragments, which are rolled
along with the previous ones; the water freezes, and, on breaking up in the spring with the
melting snows from the higher grounds, forms an impetuous flood, which drives all before it
in one general mêlée. In this way the angles are soon worn off, and every successive flood,
or breaking up of ice and snow, helps to transport them farther down the stream, reducing
their angles and their dimensions. In the beds of some of these streams, less than ten miles
from their source, I have seen thousands of boulders of all dimensions from a pebble to the
size of several tons. If these find their way to situations where they may be transported in
floating ice, they are already perfectly rounded; and it is easy to conceive how those previous-
ly rounded in this way may be intermingled with angular fragments which have not been
subjected to attrition, and both be deposited together, . -
Means of transport, conditions, etc. of the surface.
We have now to inquire by what means these blocks have been removed to their present
position; and whether we have any other knowledge of the conditions of the surface at this
period, which will enable us to decide, with any degree of probability, what agencies have
operated. . -
From the fact already stated, that these masses for the most part lie upon the surface,
though sometimes buried beneath the drift, we are led to the conclusion that they were not
moved by any powerful flood, such as has sometimes been supposed; for, in this case, they
would inevitably have been mixed with the loose materials of the surface which underlie them;
and if a flood, with a force sufficient to transport these masses, had passed over the surface,
the whole superficial deposit previously existing would have been swept off. Without the
necessity of any farther reasoning in this place, we are led to adopt the opinions advanced by
numerous writers, and supported by modern analogies, viz. the transportation of blocks of
granite and other rocks enclosed in masses of ice. * -
In all situations where glaciers from mountain regions come down to the sea, they float off
in large masses, and even great tracts, bearing with them the accumulated fragments of rock
and earth which they have gathered up in their passage. River and lake ice may do the
same at the breaking up of a northern winter; and in this manner large quantities of rocks
and earth are annually transported many miles from their original position, to be deposited
only when the iceberg shall be stranded upon some coast, or the bottom of a shallow sea; or,
passing into a warmer climate, it is gradually melted, and precipitates its load to the bottom.
This subject is ably treated in Mr. Lyell’s Principles of Geology, and in the concluding
portion of Mr. Murchison's Silurian Researches. - -
It remains for us to inquire what were the conditions of this portion of the continent at the
period in which these boulders were transported, and whether modern analogous conditions
NORTHERN BOULDERS. - 335
offer any evidences to lead to a belief that glaciers were formed on our northern mountains;
that moving down to a sea then covering a large portion of the country, they floated off with
their loads of earth and boulders, which have been precipitated over the whole of New-York.
When we examine these boulders, we are naturally led to ask, whether they are of the
kind of rocks previously familiar to us in place, and if they can be referred to any known
primary mountains; for if we can once fix their original locality, we are better prepared to
offer explanations of their mode of transport. A large proportion of the boulders of Western
New-York are of dark felspathic granite, and red granites like those of the northern part of the
State. Some of other varieties occur, which are likewise referable to the same region. A
few of crystalline limestone with serpentine have been found; and these are so precisely like
a rock of that kind in St. Lawrence county, that we are inclined to refer to that place as its
original home. A few boulders of specular iron ore have been found among the most extreme
southwesterly materials of that kind; this is precisely like the ore from numerous points in
St. Lawrence county. These are a few of the analogies which might be enumerated.
By casting the eye over the Geological map, it will be perceived that the northeastern por-
tion of the State is occupied by a great central nucleus of Primary rocks, consisting of dark
and reddish felspathic and other granites, crystalline limestones, etc.; this extends, though
somewhat interruptedly, into Canada. The elevation of a large portion of this country is from
two to four thousand feet above tide water, and many of the higher peaks approach to the
elevation of five thousand feet above the level of the sea.
Admitting that the relative elevations between this part of the State and Western New-
York have remained the same, the greater portion of the latter may have been submerged
beneath the ocean, and still there would be large tracts of the former elevated two thousand
feet above its level. If, under these circumstances, glaciers were formed upon the sides of
these mountains, and descended to the sea, many of them would be carried forward by the
oceanic current far into that part of the ocean which then occupied western New-York. Even
the accumulations of snow and ice during winter, in the streams flowing from these islands,
would, on the breaking up in spring, carry forward large quantities of loose stones. The same
is shown by Capt. Bayfield to take place on the breaking up of the lakes and streams of the
St. Lawrence valley at the present time; and we are warranted in supposing a more severe
climate under the conditions suggested, as known by comparison in other latitudes.
From observations in the southern hemisphere, Mr. Darwin has shown that a larger pro-
portional area of water is accompanied (probably as a consequence) by a more equable climate,
the presence of tropical productions, and at the same time a low limit of perpetual snow, and
therefore the descent of glaciers into the sea in latitudes as low as 46° 40'." This reasoning
he has illustrated by some beautiful comparisons between places in the southern hemisphere
and different parts of Europe. These facts he has undertaken to apply to the explanation of
the geological phenomena of the transportation of boulders and fragments of rock included in
* Darwin's Journal, quoted by Mr. Murchison, Silurian Researches, p. 542.
336 GEOLOGY OF THE FOURTH DISTRICT.
masses of ice. The facts observed, which establish the proposition of a low limit of perpetual
frost, with a luxuriant vegetation, and islands covered with eternal snow, while the sea in
the same latitude swarms ‘with living creatures,’ can be applied to this portion of the world
as well as to Europe, and furnish us with the same arguments in explanation of the transport
of boulders. - -
Let us now go back to the consideration of the condition of these boulders, and their relative
situation to other superficial detritus, and we shall find that there can be no explanation offered
of their mode of transportation, except during a time when the whole surface was covered by
water. Had they been transported by a powerful current over the bottom, (which cannot be
supposed from the inequalities of the surface,) all the older drift would have been removed at
the same time, and instead of finding them as we now do mostly upon the surface, they would
have been imbedded indiscriminately in the superficial detritus, and there would have been no
means of recognizing the products of different periods. -
In order to allow of a sufficient depth of water for the transport and deposition of these
boulders in the places we now find them, it would require a depression of the country from
five hundred to two thousand feet below its present level. This greatest depression would
cover nearly all of the middle and southwestern portions of New-York, and the whole extent
of country occupied by the Great lakes, a large portion of Canada and the Western States.
Indeed, allowing the relative elevation of different portions to have remained the same, which
as regards New-York is doubtless true, the whole of that portion of North America east of
the Rocky mountains would be one great ocean, with numerous and thickly scattered islands.
The mountain chains of New-England and New-York would form long ranges of islands
rising from the ocean to two and three thousand feet above its level, their sides covered with
perpetual snow and glaciers, and their bays terminated by cliffs of ice, from which detached
masses floated off, bearing with them boulders and fragments of rock.” These would be
transported in every possible direction by the ocean currents; and wherever the mass became
stranded, or when it passed into warmer latitudes, its load of earth and rocks would be
deposited. -
To a certain extent, this view is corroborated by the dispersion of the boulders in New-
York; for we find them on every side of the great primary nucleus before noticed, and those
found many miles north of this point are undistinguishable from many of those at the south.
Still it must be acknowledged that the greater number seem to have been transported south-
ward, probably owing to the existence of a polar current as in the present ocean.f It is not
only probable, but it can be demonstrated, that this dispersion of the boulders and fragments
continued for a long period, and while the land was rising from the ocean, and the gradual
* See Darwin's Journal, page 291 et seq.
# I am informed by Dr. Emmons, that although there is no lithological difference in the transported blocks on the St. Lawrence
at the north and northwest, as well as at the west and southwest, of the Great Primary region of New-York, still they diminish
rather than become more numerous on approaching the base of these mountains, while the reverse is true when we attempt to
trace their origin from the South. -
NORTHERN BOULDERS. 337
elevation of some portions above water might produce counter currents; and finally, after the
land had risen to within eight hundred or one thousand feet of its present elevation, the great
valley of Lake Ontario would form a broad bay, communicating with the ocean through the
valleys of the Mohawk and the Susquehannah, while the communication by the valley of the
Mississippi was becoming closed. Even for a long period after this, the bay of Lake Ontario
would communicate with the ocean by the valleys of the St. Lawrence and the Mohawk,
while the valley of the Hudson formed a narrow strait, with numerous inlets and bays; the
granite mountains of Northern New-York and of the Highlands, and the old red sandstone of
the Catskills, rising to the height of from two thousand to four thousand feet above its level.
I have enumerated only those mountainous regions of New-York and New-England with
which I am familiar. Of the elevated country in Canada, north of Lake Ontario and the St.
Lawrence, too little is known to speak with certainty; but it is extremely probable that this
also has furnished its share of the transported materials, which we now find in the valley of
Lake Ontario and Western New-York, Farther west, there remains no doubt but the country
on the north of the great lakes has furnished the boulders of Ohio, Indiana and Illinois; and
as these mountains become more elevated toward the sources of the Mississippi and farther
to the northwest, they have been the source of a much greater number of boulders over the
country west of the Mississippi, than farther east.
We have also to inquire what collateral proof we have of this condition of the continent,
besides the dispersion of the boulders. I have before alluded to the deposits of newer tertiary
extending through the valleys of Lake Champlain and the St. Lawrence, which contain marine
shells of species existing in the present ocean. Similar deposits, but without the shells, exist
in the valleys of the Hudson and Lake Ontario. These have been subsequent to the great
abrading and denuding agency which has excavated the valleys and scored the surface of the
rocky strata, and previously to, or in part formed during the period of the transportation of
the granitic boulders. - - - ."
This Tertiary deposit on Lake Champlain is elevated in some parts nearly three hundred
feet above the lake, which shows a depression of the present level, at the time of its formation,
at least four hundred feet. This would be sufficient to raise the water of the ocean about one
hundred and seventy feet above Lake Ontario, or nearly to the elevation of the ancient ridge
bounding that lake." The boulders of Primary rocks are distributed over the surface of this
fossiliferous deposit, and in some places imbedded in it. In speaking of their occurrence in
the tertiary of the St. Lawrence valley, Capt. Bayfield says, “They are found in the cliffs at
different levels, not resting upon each other, but as if they had been dropped there at widely
different times, during a long period, in which a quiet deposition of clay, sand and gravel had
been going on, and in which the different genera of testacea had lived and died. Some of the
shells are of course broken, and some of the valves are separated, as is the case in the bottom
of the present sea; but many have both valves together, although they separate when taken
up, because the ligament no longer exists. All idea of these shells (together with the sand,
* The level of Lake Champlain is ninety-three feet above tide water.
[GEOL. 4th DIST.] 43
338 GEOLOGY OF THE FOURTH DISTRICT.
clay and boulders) having been drifted together into their present positions, must be given up
at once, when I state the fact, that the Terebratula psittaceae, which you know are so fragile
that the smallest stones would be sufficient to destroy them, if carried along with a moderate
degree of violence by moving water, are found with their valves together, and their long and
brittle teeth entire as when they were living.”
The inference of Capt. Bayfield, that “these numerous erratic blocks have been dropped
from time to time, from ice floes, on the bed of the Tertiary sea,” is substantiated by all the
facts observed; and we have already shown from what sources these boulders may have been
derived, at a period when large portions of the present continent were depressed beneath the
ocean level, and when the conditions of climate were favorable to the production of large
numbers of living creatures on the bottom of an ocean, in the vicinity of islands almost
‘wholly covered with everlasting snow.’ - -
It is unnecessary here to follow any farther these deductions. The deposits of newer
tertiary along the New-England coast show, conclusively, that all this region was equally
depressed with that of New-York; and the presence of boulders there may, to some extent,
be accounted for in like manner.
The elevation of the tertiary of New-York, or New-England, is not sufficient to explain
the transport of boulders to situations fifteen hundred or two thousand feet above tide water,
if we admit the ocean to have been only at sufficient height to allow of that deposit. But
having proof of the conditions necessary for the transportation of boulders at this period, shall
we not be warranted in carrying backward these conditions to explain the means of transport-
ing those found at higher elevations, when the sea covered a much larger proportion of the
land; and when, perhaps, the climate was less favorable to the production of living beings
on the bed of the ocean? - - - - -
The facts stated seem very clearly to establish distinct and widely distant periods between
the formation of the great body of the drift in Western New-York, and the erratic blocks or
boulders. These products have often, and indeed almost always, been confounded with each
other; and the whole accumulation of superficial detritus, except perhaps the finer alluvia
along river banks, has been considered as the product of a single period. It will be seen,
also, that the scoring and polishing of the rocks has taken place at a period long anterior to
the transportation of these northern boulders, and that their passage over the surface has had
little or no connection with this phenomenon.
The production of the local or older drift in the Fourth District was, probably, caused by
the elevation of the great mountain chains on the north and east ; which, by uplifting and
disturbing the sedimentary rocks far to the south, gave origin to those partial dislocations
and undulations which have been noticed. At the same time the violent movements thus
produced elevated the edges of the strata, uplifting, overturning and pressing them forward,
with their load of detritus, as represented in the section, Plate VIII. I might go farther
into an explanation of similar phenomena, which are developed over the whole extent of
* Extract of a letter from Captain Bayfield, R. N. to Mr. Lyell. November, 1837. (See Appendix to Silurian Researches.)
NORTHERN BOULDERS. 339
Western New-York; but I have already devoted more space than was intended to this sub-
ject, upon which, although there are an immense collection of facts, there is yet no universal
mode of explanation. .
The great difficulty has been in the attempt to find some one cause which would satis-
factorily account for the whole, while no attempt has been made to recognize the products
of successive periods. The idea of a universal deluge, early inculcated, and strengthened
by the arguments and facts brought forward to sustain the opinion, has led to the general
belief that all superficial deposits were due to a single period, and to one agency. Geologi-
cal phenomena are now studied without reference to preconceived opinions or interpretations,
and by adopting more natural and rational explanations than otherwise could be done, we
escape advocating numerous absurdities, without conflicting with religious opinions. No
geologist, at the present time, can use the term diluvium in connection with the deluge of
Scripture history, or refer the superficial detritus of a country to the same agency.
In many instances the relative position of the Great Boulder formation, and the more
ancient drift, is well illustrated in the natural or artificial sections of these deposits. It must
be acknowledged that there are often huge unworn fragments of the rocks of the district
mingled with the granitic boulders, but these rarely extend many miles south of the outcrop-
ping edge of such masses. The following example is a section of a hill in the town of Victor,
Ontario county, on the line of the railroad :
Section of Drift and Boulder formation, Victor, Ontario county.
The lower deposit is of fine and coarse sand, with pebbles of the rocks of the district, dis-
tinctly stratified; this is succeeded by an unstratified deposit of coarser materials, consisting
of large and small pebbles and boulders of granite, and other rocks with intermingled clay
and sand. With this deposit are some large irregular fragments of limestone from the upper
part of the Onondaga salt group, which have been transported only a few miles. It is evident
that at the time this heterogeneous mass was brought upon the lower deposit, it suffered
denudation to a considerable degree, the upper layer of sandy loam, with some of the coarser
materials, having been removed on one side. Numerous similar deposits have been observed,
and indeed they are among the most common appearances of the drift hills.
43* . . .
340 - GEOLOGY OF THE FOURTH DISTRICT.
The hills covered with drift along the south side of the Ridge road, and upon the shore of
Lake Ontario, exhibit very similar phenomena. Some of the bluffs on the lake shore present
large accumulations of clay and gravel above the boulders.
º
| #."
º
| i
††
fift||||||||
& aſſi | º | º,
º
ſº
EE-
*ś Tuº tº. ńºš
. zº ºlº - ? & §§ - ſ % - % *†† - * --- *** SS
- / f : # - ſ * |lºſſº ji. §§§ *
/ | i. ^ # - | %'º' ſº , it |; § § º f M
&b Go tº ſº e= ſºlºi.
====E==
º § } º º º |m.
Hºed i. |
The illustration above is from a bluff in Monroe county, on the lake shore. The lower
stratified deposit consists of gravel and loam, which is succeeded by a range of granitic
boulders mingled with clay and gravel, and covered to the depth of several feet more with
gravelly clay. The lower stratified deposit is evidently the product of a period distinct from
that above, which presents no lines of stratification.
The bluff has been undermined by the action of the waves, and trees and stumps have been
thrown, and often remain standing upright in the beach below; and at a cursory examination,
many of them might be supposed to have grown there, so deeply imbedded and firmly are the
roots fixed in the sand and pebbles. - - -
Huge blocks of the Medina sandstone are sometimes found resting on the top of the Niagara
limestone; these are scarcely worn, and appear to have been lifted from the upper outcropping
edge of the mass, and dropped upon the limestone above. In like manner, numerous masses
of the Niagara limestone are drifted forward, resting on the Onondaga salt group. Upon the
terrace formed by the Corniferous limestone, we find great numbers of immense blocks of
limestone from the upper part of the Onondaga salt group. This portion has been before
described as an impure argillaceous limestone, in strata of ten or fifteen feet thickness. These
masses frequently lie in their original position, as if the edge of the stratum had been enclosed
in a mass of ice, which an advancing tide carried forward and dropped upon the bottom.
The unequal hardness in different parts often causes them to be worn into fantastic shapes.
NORTHERN BOULDERS. - 341
t
There were formerly several of these on the road from Caledonia to Batavia, but the following
is the only one now remaining, which presents much of interest:
165.
==
------ * ſ tº
*==eſ
ź. º {{ſ |
A_º }
E. ſº =# = sº
[.
3
\\ſ! . V2ſ.
=#E:\º
º
5-5
º º: sº
㺠º:
* *. -
team?:
Transported block of Hydraulic limestone, near Batavia, N. y.
&
The upper and lower portions have resisted the action of the weather, while the central
part has wated away. There was formerly another one near this locality, but the upper part
has since fallen down.” - - -
In connection with this subject, may be noticed the direction of drift hills, as they occur in
the eastern part of the district. In many places these hills have no definite direction, but all
those north of the great valleys of Seneca and Cayuga lakes have a peculiar form and determi-
nate direction. They are long, elevated ridges, rising abruptly on the north, and sloping gra-
dually down to their southern termination. The ascent from the south is almost imperceptible,
and often scarcely noticed, till one observes himself on an elevation of fifty or sixty feet above
the valleys on either side. I have been informed by the engineers in this part of the country,
that a line may be run for a long distance, upon the summits of these hills, having a direction
N. 10° E.; and from numerous observations, this appears to be the prevailing direction.
It will also be seen that this direction corresponds very closely with that of Seneca and
Cayuga lakes. The form of the hills is precisely such as would be made by a powerful cur-
rent passing southward through these valleys, piling up the coarser materials at the northern
extremity, and moving the finer ones farther on, until they were in some measure protected
by this barrier before they were deposited. It is quite evident that this took place after the
formation of the valleys, and probably at the period of, or subsequent to the boulder deposit.
The materials are often mingled in the greatest confusion, though there seems to have been
subsequently an equilibrium of the currents; for there is in many places a regular deposit of
fine sand, and in the valleys one of clay covering the coarser products. …”
* May it not be possible that some operation of this kind may produce the “rocking stones,” which are such a marvel? If the
mass wearing away be thin, and those above and below are unaffected by weather, the one may be very nicely poised upon the
other, as the matter between is slowly removed.
342 GEOLOGY OF THE FOURTH DISTRICT.
#########
É=#:
############# :
E:º->
Alluvial hills and terraces on the Conhocton valley, as seen from Liberty corners. From a sketch by Mrs. HALL.
CHAPTER XIV.
MODERN SUPERFICIAL DEPOSITs.
After the period of the superficial deposits just described, and when the surface had be-
come permanently elevated above the ocean, its inequalities would give origin to broad lakes
and rivers, discharging themselves into the surrounding sea. By any irregular motion attend-
ing the farther elevation of the land, and even from the accumulation of water alone, the bar-
riers of these lakes might be broken down, their beds deepened, and vast quantities of detritus
carried to the lower plains, or into lakes or rivers at a lower elevation. That such has been
the condition of the whole of New-York, will admit of demonstrative proof, and the details
of the various modifications of this modern period would occupy many chapters. In many
instances it requires much careful examination to separate the products of this period from
those of previous ones, and also to recognize the different ages of modern deposits; for
these again are, among themselves, referable to distinct epochs. We can only select a few
well defined examples, and such as are produced by causes that will at once be recognized;
leaving a consideration of the whole subject, and the various and successive changes, to some
future opportunity.
MODERN SUPERFICIAL DEPOSITS. *-- 343
There are numerous points where the accumulation of superficial detritus is local in its
character, and very circumscribed in its limits. These deposits often consist of an inter-
mixture of the older drift, with boulders which have been removed by the change in the
course of a river, the bursting of a lake, or some other phenomenon of the kind. They are
recognized by numerous characters; but a general distinctive feature is that of containing
materials of both northern and southern origin, confusedly intermingled. They often rest
upon previously formed superficial detritus, and are distinguished by position, as well as by
the character of the materials. Several cases of this kind have been enumerated in the
Annual Reports; and many others might be added to the list, were it necessary to increase
the number for the sake of illustration.
In passing along the margins of the broad valleys, such as the Genesee and others, we
find, opposite the mouth of every stream or deep ravine entering the valley, a mound of
greater or less extent, and undistinguishable, upon the surface, from the surrounding deposits
of similar nature. Occasionally, however, the bursting of a cloud, or a powerful spring flood,
reveals to us the mode of these formations, in the production of mounds of earth, pebbles and
fragments of rock which are swept down by the resistless torrent, and heaped up as the
stream emerges into the broader valley. The more ancient deposits of this kind often cover
many acres, and, from all the analogies, we must suppose that they were formed in the same
manner as recent ones of the kind. Sometimes, however, it appears as if a lake may have
burst its barriers upon the high ground, and the waters suddenly discharging, have carried
forward this immense mass of materials. These deposits often occur opposite the inlet of
ravines in which no water flows at the present time. -
In many of the river valleys the accumulation of materials indicates the whole to have been
occupied by a deep lake, and that the fine sand and loam has been brought down by streams,
and spread over the bottom. Terraces are often left at successive points, indicating the stages
of recession in the waters occupying these lakes, as the outlet has been lowered.
In the valley of the Conhocton, opposite the junction of the valley of the Canandaigua lake,
there are several successive terraces, as represented in the woodcut at the head of the chapter.
It would appear that at the same time in which the current was flowing down the valley of
the Conhocton, a still more powerful current, probably loaded with detritus, came in by the
valley from the north, and was carried against the south side, when these materials were
deposited in the eddy current, while the stream turned its course to the east.
Along the courses of nearly all the streams and rivers, we find evidences of their having
once stood at a higher elevation than at present. These evidences consist in long terraces of
pebbles and sand, often successively repeated; and from being continuous, and at the same
elevation for long distances, no farther facts are required to indicate their nature. It would
require too much space to describe all the examples of this kind which have been examined.
A few of the more extensive and important cases will be noticed.
The deep depression known as the Genesee valley, extends from Rochester, southward, as
far as Dansville. Following the same direction we find, after rising several hundred feet,
344 GEOLOGY OF THE FOURTH DISTRICT.
zº
that this valley communicates with the valley of the Canisteo river, and thence with the
Chemung and Susquehannah. The Genesee river, beyond Portage, flows in a valley more
than five hundred feet above the same, after leaving the gorge at Mount-Morris. The
northern part of this valley, from Rochester to Dansville, maintains nearly the same elevation
throughout, or with a gradual descent to the north. It is one of the most ancient valleys of
excavation; and its sloping sides, covered with superficial accumulations to the height of 600
or 800 feet above its base, show an immense period of time to have elapsed since its forma-
tion. Long subsequent to its formation it has been partially filled with water, having a bar-
rier on the north, and extending over the whole plain of the “Genesee flats,” and south as far
as Dansville, in one great shallow lake. At the same time the valleys south of Dansville and
south of Mount-Morris, by way of Cashaqua Creek, were discharging their waters into this
lake. With these streams was brought down a large quantity of coarse and fine materials,
which we now find about Dansville, and below the junction of the Cashaqua creek, while the
great extent of the valley is spread over with a fine sandy loam. The materials are precisely
like those which are carried into modern lakes, by their tributaries; and when they are filled
nearly to the surface, a growth of vegetation ensues, changing as the whole becomes drained.
An examination of this deep deposit, on the Genesee flats, shows conclusively that it has
been made in a lake, such as described, with a current passing through it from south to north.
The deposit was evidently carried forward in that direction, as indicated by the lines of lami-
nation. The coarser materials, at the points mentioned near the embouchures of the streams
into this lake, are, in considerable proportion, of southern origin.”
The former outlet of this valley appears to have been by the Irondequoit; but this becoming
obstructed with the vast accumulations of Superficial detritus, it sought another course, and
excavated a channel by way of Rochester, which, as it has been worn down, has gradually
drained the lake, leaving the present flats as its ancient bed.
The valley of the Genesee south of Portage seems to have been in a similar condition with
that portion on the north, except that from the proximity of the hills on either side, a larger
proportion of coarse materials has been distributed over the bottom. At the junction of the
Angelica creek with this valley, there is the clearest evidence of its condition at that period.
From the direction at which that valley joins the valley of the Genesee, the stream flowing in
would extend across to the western side, depositing its coarser materials, while the finer
sediment of clay and sand would be deposited in the eddy formed by the junction of the two
streams. Accordingly we find below the junction of this stream an extensive deposit of sand,
loam and clay, chiefly of the former; and its extent is marked in some degree by the growth
of evergreen timber. -
* As an example of this kind, may be noticed the accumulation of gravel and sand, resting on regularly stratified clay, at
Squakie hill, near Mount-Morris. The excavation of the Genesee Valley canal has exposed a deep section at this place,
showing the lower deposit of fine clay horizontally stratified, and succeeded by a stratum of coarse pebbles and gravel, and
above this loose sand and gravel the ruins of rocks on the south. This example shows an inundation of these materials after
the deposition of clay and loam forming the Genesee flats.
MoDERN SUPERFICIAL DEPOSITs. 345
In the vicinity of Portage village, we find an immense deposit of coarse sand and gravel,
piled upon an older deposit of sand and clay; showing, subsequent to the period of the ancient
drift, and after the great deposits of clay and sand following it—indeed apparently subsequent
to the boulder period—a condition of things producing this immense local accumulation.
The lower deposit is regularly stratified, and consists in part of materials of northern origin.
This appears to have been partially excavated, and another deposit spread over it, of materials
from the south, consisting of flat masses of sandstone and scarcely worn pebbles, with loam
and gravel." It is entirely distinct from the formation below, and proceeded from a long
subsequent operation. It will be farther alluded to in connection with the recent production
of valleys and river channels. - - -
The excavation of the Genesee Valley canal has given an opportunity of examining these
deposits in a very satisfactory manner, and many facts have been brought to light. The
surface alone, or the natural banks of the river, offer no opportunities of investigation.
In the broad indentation on the eastern side of the river, opposite the middle falls, the canal
passes along the slope of the hill, which rises nearly two hundred feet higher. The lowest
deposit excavated at this point consists of alternating layers of clay and quicksand, which,
about one hundred feet lower, rest upon the rocks of the Portage group, as illustrated in the
following section: s - : * - ;
S
s
--~~
Es
TsºF. T= SEF
- * — -
*~. ºf ~' -- .N. Q->
s's ‘-E SSSF
& *~~ & ~ ~x.
+: --> -: – S :
S- . = s.s - ſ
* . . . -- ~~
sº S.S.; "... *
* * * *
--> JSS tº -
~S.RSS * Sº, ~" §
“s- sº-
s's *
Section of the hill at Portage tunnel.
#3
1. Shales and sandstones of the Portage group. s.
2 & 3. Regularly stratified deposit of clay and quicksand. -
4. Materials similar to those below, with fragments of trunks of trees in the lower part.
5. Gravel and sand, having a large proportion of its materials of southern origin.
a b, c. A superficial deposit, formed by the undermining of the hill above.
a. The point at which the Genesee Valley canal is carried around the hill.
* See Annual Report of 1840, pp. 439 and 440.
[GEOL, 4th DIST..] 44 -
346 GEOLOGY OF THE FOURTH DISTRICT.
This deposit of clay and quicksand extends about one hundred feet above the level of the
canal, where it is succeeded by sand and gravel. For more than two hundred feet from the
bottom, the mass consists of alternating layers of sand from two to eighteen inches, with layers
of clay of half an inch to two inches, each becoming thicker as we approach the upper part,
where the quicksand layers are fifteen and twenty feet. - - . . .
The upper layer, of fifteen feet thickness, becomes perfectly saturated with water, and is
termed liquid quicksand; and this is succeeded by the deposit of coarse sand and gravel,
which is of subsequent origin, containing materials from the rocks of the south, mingled with
some of the older drift deposits which have been broken up. Through this the water perco-
lates, saturating the mass below, and giving it the character of quicksand. -
Fragments of the trunks of trees have been found in this deposit, in a layer of clay about
thirty-five feet below the gravel." - -- -
The whole of the lower deposit, consisting of regularly alternating layers of clay and sand,
was evidently deposited in a quiet lake, while the subsequent one of gravel and coarse sand
was brought on by some powerful inundation from the south. The fragments of wood are
doubtless such as were drifted from the higher grounds into this lake, and sinking to the
bottom, were covered by the subsequent sediment. -
In several similar situations, bones of the mastodon have been found, and consequently
referred to the period of the drift. These facts, however, offer no arguments in favor of such
an hypothesis; for in all instances which occur in Western New-York, there is the strongest
evidence of their having been transported from their original situation, and mingled with the
more modern fluviatile or lake deposits. ". -
Another circumstance to be noticed in connection with this section, is a superficial deposit
(a, b, c) of about ten feet in depth, covering the whole slope, from the base of the gravel hill
to the bank of the river. This surface deposit is composed of the ruins of the gravel hill,
with the clay and sand below. From the constant oozing of water from the lower deposit,
it undermines that above, which falling, carries with it something of those below, the whole
constituting a moving mass, saturated with water. Its nature only became fully under-
stood upon the excavation of the canal, when all that part above commenced sliding down,
completely destroying the work. Farther examination proved that the whole hill side, for
ten feet in depth, was in motion towards the river, and of course no excavation or fixture
could be made permanent on such a foundation. In proof of this, and that such, for a long
period, has been its condition, we find that the oaks which grow upon the hill, towards the
top, have slidden down to the rocky margin of the river, where they stand among the hem-
locks and cedars, sometimes upright, but often leaning in various directions.
t
a-
* I am indebted to Col. Elisha Johnson, of Hornby Lodge, Portage, for numerous facts relating to this section, as well as for
specimens of the wood, which was dug out under his direction. This wood has been examined by Prof. Bailey, of West-Point;
but from its condition, he has been unable to decide its nature. -
.*
-. MODERN SUPERFICIAL DEPOSITS. 347
The whole surface, for half a mile, is saturated with water, and springs gush out at every
step. We see very plainly how fallacious would be any reasoning as to the nature of these
deposits from what appears upon the surface.
A similar modern deposition at Goat island, on the Niagara, will be described, in connection
with the falls and river channel. Numerous local deposits of this character, of greater or
less extent, can be found in nearly all the ancient valleys of the Fourth District, but it would
occupy too much space to describe them. They are often, and generally due to similar
causes with those above detailed. It appears as if, after the elevation of this region from be-
neath the sea, extensive lakes were left upon some of the higher grounds occupying broad
depressions; and that these have frequently burst their barriers, producing local depositions
of gravel and coarse sand along their outlets or in the valleys below.
*-
44*
348 GEOLOGY OF THE FOURTH DISTRICT,
CHAPTER XV.
LAKE RIDGES.
Ridge roads of Lake Ontario and Lake Erie—Terraced hills—Modern lake ridges and
beaches.
One of the most interesting of the superficial deposits of the district is the “Lake Ridge,”
which, from Sodus in Wayne county, with some trifling exceptions, is a travelled highway,
nearly as far as the Niagara river. Beyond this it can be traced quite to the head of Lake
Ontario; and I have been informed that it exists upon the northern side of the lake. Through-
out its whole extent in New-York this ridge is well defined, except from slight interruptions
caused by the passage of streams. It bears all the marks of having been the boundary of a
large body of water, and of having been produced in the same manner as the elevated beaches
bordering the ocean or our larger lakes. The ridge follows the general course of Lake On-
tario; being, at its nearest point, about three miles distant; and at its greatest, perhaps less
than eight miles.
In some places it is strongly defined, descending toward the lake twenty or thirty, and
even fifty feet, in a moderate slope. Its seaward side is usually covered with coarse gravel,
and often with large pebbles, resembling the shingle of the sea beaches. The top is generally
of coarse sand and gravel, though sometimes of fine sand, as if blown up by the wind, similar
to modern beaches, when the coarser materials are thus left as the waves deposit them, while
as the finer parts become dry they are carried to a higher elevation. It is sometimes so
contracted upon the top as to offer only space for a broad carriage road, and again expands to
a width of two or three hundred feet, being scarcely defined on the inland side. It is far
from uniform in height, and in passing the distance of a mile inequalities of several feet may
be perceived; still this feature is only an exception, and when the road is tolerably direct, a
traveller may be seen as far as the eye can reach. Neither is this a single continuous ridge,
but often divided into several, running parallel to each other, and again uniting in one.
All these deviations in height, breadth, continuation, etc. only the more forcibly impress one
with the idea of its analogy to existing beaches, where we observe the same inequalities. In
looking from the ridge toward the lake, the uniform surface of the country and gentle slope
* The term lake ridge is used to distinguish it ſlom the terrace formed by the outcropping edge of the Niagara limestone,
which is known as the “Mountain Ridge.”
LAKE RIDGES. 349
remind one very strongly of the high sea beaches of pebbles and sand bounding many of our
Atlantic bays, where, when the tide is down, he can see over an extent of miles of almost
level sand and mud.” - - - - -
If any thing were wanting in the external appearance of this ridge to convince the observer
of the mode of its formation, every excavation made into it proves conclusively its origin.
Fragments of wood, shells, etc. are found in digging wells, and cutting channels to drain the
marshes on the southern side. I have not had an opportunity of seeing any of these shells,
but have no doubt of their existence. In the town of Cambria, Niagara county, I was fortunate
enough to find a recent excavation entirely across the ridge, cutting down to the level of the
country on the south. The lowest deposit is a coarse sand or gravel, and upon this a regular
deposit of silt and thin fragments of wood. Some of the latter, which are branches or roots
of trees, have in parts entirely lost their woody structure, have become brittle, with a close
grain and dark resinous shining fracture, and present, in fact, an appearance more like highly
bituminous coal than any other substance. In some parts again the woody structure is more
perfectly preserved, but still presents an appearance like lignite. The layer of vegetable
matter is evenly spread, as if deposited from water, and afterwards covered with fine sand;
to this succeeds coarse sand and gravel. -
This example leaves no doubt of the mode of formation, if indeed any proof of the kind
were wanting. I have been informed of numerous similar instances, though no other has
fallen under my own observation. j
In its eastern extension in the town of Sodus, this ridge ceases to be well defined. It will
be observed that this point comes within the range of the valleys of Cayuga and Seneca lakes;
and I have before remarked, that all the drift hills have a direction toward these valleys. The
present level of Seneca lake is somewhat above the Ridge road, and that of Cayuga lake is
below it. - , - -
At the time when the water of this lake or bay was at a higher elevation, it doubtless
communicated with the valleys of Seneca and Cayuga lakes, and even discharged southward
through these valleys, as indicated by the direction of the hills before alluded to. At a sub-
sequent period there have been deep bays and marshes along the margin of Lake Ontario,
which are still represented in the eastern part of Wayne county. These, with the water
discharging into the lake from the higher grounds, prevented the formation of any distinct
ridge; and still farther east through the valley of the Oswego river, Lake Ontario, at the time
of the formation of this ridge, must have communicated with the Cayuga lake.
The interruptions in the continuity of the ridge, from the passage of small streams, are
numerous throughout its whole extent. Many of these streams were doubtless discharging
their waters into the lake at the time of the formation of this ridge, and have thus kept an open
• To the geological reader it will require no attempt to prove this the ancient beach of Lake Ontario, or a body of water,
perhaps an arm of the ocean, which once stood at this elevation; such occurrences are well known elsewhere; but there are many
persons in western New-York, and some grave critics among the number, who prefer to explain this by supposing some stupen-
dous uplifting of the strata in this line ſcom Sodus bay to Niagara river. -
350 GEOLOGY OF THE FOURTH. DISTRICT,
passage; others have been closed up during its deposition, and formed little ponds upon the
inland side, which, subsequently becoming powerful, have burst through the barrier, and carried
away large portions of it. The original elevation and extent of many of these ponds on the
south side of the ridge is still distinctly marked, although there is now but an insignificant
rivulet flowing in their channels. - -
The most important interruption in its course is at the entrance of the Eighteen-mile creek,
in Niagara county. In passing from the east, we find, before reaching the creek, that it bends
around to the south, showing that a bay extended inland along the course of the stream.
After this there is no well defined ridge for four miles westward, where it again commences,
and continues without interruption nearly to Lewiston. All these facts are highly interesting,
as showing its analogy to modern beaches along the lake shore, and the effects of streams
flowing in from the higher grounds. ~} - -
In the town of Cambria, Niagara county, this ridge divides, or perhaps, more properly, we
find a ridge diverging from the main one, and pursuing a northwesterly course for several
miles, when it becomes merged in the general surrounding level. The main ridge, in the
mean time, pursues its regular course, apparently uninfluenced by this diverging one.
The following diagram illustrates the position of these ridges: ~, -
168.*
—-"T-
--F-TF
º
º
- ==º
§§Wº"
º \
& Sºº W |||}}} º *) \ | - •
*º-
gº º
-º !!! -“” => *===
––Pº I | li Žº.
|
=º
—-
The smaller one is known as the “Little ridge,” from being less than the other; it is a
single low well-defined ridge sloping uniformly on both sides, the country around being nearly
level.f
* See note under Modern lake ridges, page 356. f
# This feature of sloping on both sides, has been urged as an objection to the main ridge having been formed by the lake, as
beaches are supposed to slope only seaward. Such, however, is not true either of lake or sea beaches, where they are formed
before low or level ground; there is always a ridge sloping inland, as well as seaward, and elevated in proportion to the force of
the waves and its position with regard to accumulation of materials. I could cite an example on Massachusetts bay, where the
sea has thrown up a beach for the distance of two miles, and from twenty to forty feet above its own level, completely damming
out a large marsh about its own elevation. The water from this marsh finds its way into the bay by a circuit of ten or fifteen
miles. Precisely similar were the operations in the formation of this ridge ; and analogous operations, only upon a smaller scale,
are going on along the present lake shore. | -
LAKE RIDGES. 351
The elevation of this ridge above Lake Ontario has been variously estimated from one
hundred to two hundred feet. In 1838, through the kindness of Mr. Barrett, I obtained the
elevation of the ridge north of Lockport, which is about one hundred and sixty feet above
Lake Ontario; and very recently, Mr. Fay, the resident engineer at Lockport, has obligingly
furnished me with the following levels: * --
The Ridge road, opposite Lockport, is below bottom of canal ----------------------- 106 feet.
Opposite Middleport, Niagara county ------------------------------------- 79 tº
Opposite Albion, Orleans county ------------------------------------------ 76 (t
Opposite Brockport, Monroe county------- - - - - - - - - - - - * * * * * * * * * * * * * * * * * * * * * are sº 76 &
The bottom of the canal at Lockport is 264 feet above Lake Ontario, giving the elevation
of the Ridge road above the lake -------------------------------------- 158 feet.
At Middleport --------------------------------------------------------- 185 “
At Albion and Brockport ----------------------------------------------- 188 “”
The bottom of the canal at Brockport is about two feet lower than at Lockport. The dif-
ference in the elevation of the Ridge road at these places is readily accounted for. The point
opposite Lockport is where the ridge declines toward the Eighteen-mile creek, and is plainly
much lower than the same a mile farther east. Middleport is ten miles east of Lockport, and
the difference between the elevation at this place and the others still farther east is little more
than the difference in the elevation of the bottom of the canal.
There is a similar ridge along the country on the east of Lake Erie, commencing south of
Silver creek, and continuing beyond the limits of the State. The description of the ridge
along Lake Ontario applies equally to this, except that the country east of it is higher, and
therefore the ridge is less distinct, forming a terrace, from which one descends over pebbles
and shingle to the lower ground towards the lake. I have not been able to learn that remains
of shells or wood have been found beneath this ridge, as on Lake Ontario.
It is said that this ridge can be traced through Ohio; and the Geologists of Michigan in-
form me that a similar ridge likewise exists in that State, bordering both Lake Erie and
Michigan. The elevation is about one hundred and fifty feet above the lake level, and fresh-
water shells, with fragments of decayed wood, have been dug from beneath it.
...’
* The three last observations embrace a distance of thirty miles, in which there is only three feet of difference in the elevation
of the ridge. In Wayne county, Dr. Boyd (Annual Report of 1838) has estimated the elevation of the ridge at two hundred
feet. I have had no opportunity of ascertaining by direct measurement whether this be correct; and even allowing it to be at that
height, it varies but twelve feet from two observations in Monroe and Orleans counties,
352 GEOLOGY OF THE FOURTH DISTRICT.
Terraced Hills.
%22.
#:::::::: ==
º º-w
- X-3 ; ,
_T^- 2 ºn %
*- J.-rº. tº ~. A
_T le:º Zazzz. * *-* .
--~~~~<s --R-2.ſº 2
-** --><<SS - % =r º ---> -- >3:
--~~ ~ / zº *~~ - § e £&gº sº Sºº º
- aſ: ... " * **:Sº ś *=- f -- -------> ºrººººº-ºº: sººj §
2-TSC Tºº-s-A’ºe d t;3% * - *-ºssºs W.
- §§ § <e.
Sketch of the hill on the west side of Seneca lake valley, at Jefferson.
Besides the well-defined ridges, which can only have been made by the water of the lakes
or ocean remaining at this elevation for a considerable length of time, we often find a series
of terraces which appear to have been produced by the rapidly subsiding water. In the il-
lustration above is presented a series of distinct terraces, the surface of each with a few large
pebbles upon it. Those represented are exceedingly uniform, and below the lowest are several
others less distinct. I had at first supposed them due to the alternating hard and soft layers
of rock; but the surface is so deeply covered with drift as scarcely to allow any influence
from the strata beneath, even if the alternations were as regular as here represented, which is
not true. ^2. - -
The sketch is of the hill at Jefferson, at the head of Seneca lake, taken from the opposite,
more than a mile distant. When standing upon the hill sketched, and looking upon the opposite
side of the valley, there appears a similar series of steps or terraces, though not so distinctly
defined. Many similar appearances have been observed, but after the country becomes cul-
tivated, they are soon obliterated. The ascent from Lake Erie in many places presents these
terraces often well defined, and, by careful examination, they may afford some clue to its
successive drainage previous to the period when the well-defined ridge before alluded to was
formed. - -
The contemplation of these monuments of the former elevation of the water, and the marks
of its gradual subsidence, lead the mind back to periods when the conditions of the surface,
and the proportions of land and water, were very different from the present. If the relative
elevations of the surface in New-York have remained the same from that period to the present,
then the greater portion of the middle and eastern parts of the State would have been covered
with water. At the same period, there must have been a communication between the waters
of this great valley and the Mississippi, and with the ocean through both that valley and the
LAKE RIDGES. - 353
St. Lawrence and Hudson. These may have been successive stages in the subsidence of the
waters, under the condition supposed, during which the northern mountains formed groups of
islands, from which masses of ice with boulders were drifted over the surrounding sea, and
deposited at various elevations. This supposition seems not improbable, nor would it be
surprising if some of the remains of shells found in the ridge of Lake Ontario should prove
to be marine, thus in a measure identifying it with the period of the tertiary of the St.
Lawrence and Champlain valleys.
The elevations of the different levels of this former ocean may, hereafter, prove of the
highest interest, in connection with the theory of the distribution of boulders. The fields of
boulders between Lake Ontario and the ridge were evidently dropped upon its bed in the
most quiet manner. The thin deposit of older drift appears not to have been disturbed, and
it lies evenly spread over the strata, till we approach the ancient shore, where the waves
had sufficient power to pile up all the loose materials in one long ridge. r
From the fact that no other well defined ridge exists between this one and the present lake,
it seems that the elevation of the land was rapid; for, had there been a cessation for any con-
siderable time, the waves would have thrown up another ridge of the kind, which does not
appear in New-York.
The existence of these ridges, and others at higher elevations, though less prominetly de-
fined, give us sufficient proof of the existence of water at different elevations, and of its
gradual subsidence. These evidences have given origin to the theory of an ancient inland sea,
which formerly spread over a large portion of the territory east of the Rocky mountains, and
was limited by the great primary regions of New-England on the east. Subsequently, and
at successive periods, this sea reduced its barriers, and eventually discharged itself by the
valleys of the St. Lawrence, the Hudson and the Susquehannah, draining an immense area.
This view seems very plausible, and there are numerous facts to sustain the conclusion, but
still there are objections which appear to me insurmountable. -
The evidences of the former elevation of the inland waters remain, principally, in the
ridges and terraces of superficial materials. These are accumulated in valleys, and upon
their sides, showing them to be of subsequent origin to the formation of the river channels
and lake basins. All the great outlets being apparently of the the same date as the valleys
alluded to, it follows that this inland sea, if existing at all, had only to excavate its outlets
through the superficial detritus. From all the testimony in the case, it appears more pro-
bable that these marks of the ancient limits, which are everywhere visible, resulted from the
partial submergence of our continent after the present character of surface had been im-
pressed upon it, or from the action of water during its later elevation. These ridges are the
lines of successive emergence, and they are more or less strongly marked as they remained
for a longer or shorter time the limit of the water.
Mr. Roy, civil engineer at Toronto, Canada, has examined these ancient sea beaches with
much care; and has thus been able to establish several lines, at successive elevations, be-
tween the level of Lake Ontario and the height of 1000 feet above the ocean. From these
[GEOL. 4th DIST.] 45
354 GEOLOGY OF THE FOURTH DISTRICT.
facts, he maintains the existence of an inland sea, covering all that portion of country below
1000 feet above tide water, and that it has been successively drained to points corresponding
with the following elevations, which I have taken from a plan constructed by him.” At
some of these points the water remained long stationary, while in others only for a very short
time, the duration probably depending on the facility with which the barrier at the outlet was
reduced. r -
Above the level of the sea.
Above the level of Lake Ontario.
FEET. FEET
O ------------------------ 762 - * * * m a.º. º. -- a-- ºne ºne sº tº ºn eas - mºm sº sº tº sº ºw- - 996
L ----------------------- 680 ----------------------- 914
G ------------------------ 420 º “ - * * * * * * * * = * * * * * = = * * * * 654
E ------------------------ 344 ----------------------- 518
D ------------------------ 308 ----------------------- 542
C ------------------------ 280 ----------------------- 514
B ------------------------ 208 9 * * * * * * * * * * * * was as ºn tº sº as w = * ~s 442
A ------------------------ 108 ----------------------- 352
Level of Lake Ontario, ---------------- ------------------------------- 234:f
This theory, when connected with so many authentic observations, impressed me very
favorably; but subsequent observations have not been sufficient to convince me of its truth;
yet my examinations not having been especially directed to the subject, I may have over-
looked important facts. The fact, however, which is demonstrable, that the great valleys
of the Champlain, and St. Lawrence and Hudson, were excavated previous to a submergence
of the land, and the formation of extensive tertiary deposits, likewise proves that the ocean,
at this period, would occupy a large portion of the valley of Lake Ontario, and even, perhaps,
of higher lake valleys. These are circumstances to be taken into the account in estimating
the probability of the existence of such a sea,
Modern Lake Ridges and Beaches.
Connected with this subject is that of the modern beaches and ridges along Lake Ontario.
These are such as may be formed in the space a few weeks or months, or even during a
single storm. Some have stood for ages, and others are the sport of the changing winds and
the fluctuating level of the lake. -
Those which I have examined more particularly, are in Monroe county, and a few of these
will serve to illustrate the character of the whole. The following map, including a small
portion of Monroe county west of the Genesee river, will render these remarks better under-
stood :
* The views of Mr Roy, have, I believe, been made public in some communications to the Geological Society of London; but
I have not seen the publication, and my information is derived from his communications to myself.
# The elevation here given is three feet higher than that usually given by engineers in the United States.
LAKE RIDGES. - 355
170.
In passing westward from the Genesee, and approaching the outlet of Little pond, we
come upon a raised beach of shingle, about fifty feet wide, and extending a quarter of a
mile, separating the marsh from the lake. This slopes on both sides, and is a miniature
representation of the Ridge road. The outlet through this beach is not more than ten feet
wide, and during a storm is frequently closed. The action of the waves upon a bluff a little
east of this has been very great during the few years past. Since 1838, a portion, several
rods in width and three hundred in length, with a height of twenty feet, has been entirely
removed. The coarser materials are deposited in long lines of shingle beach, while the finer
parts are carried to a greater distance. N otwithstanding, also, that these beaches appear so
permanent, a northeast gale will, in a few hours, remove them entirely, and deposit the mate-
rials in some other situation several miles distant. In this way the outlets of streams are
dammed up, and remain until the accumulated water is sufficient to open a channel. Under
these circumstances, two or more of these ponds become united in one, overflowing the
marshes and low grounds bordering them. - -
At the time of my examinations, the outlets of Round pond, Buck pond and Long pond were
all united in one. The point a in the map, which was the original outlet of this pond, was
45*
356 GEOLOGY OF THE FOURTH DISTRICT.
entirely closed, and a long beach of sand and pebbles extended to b, the present outlet, and
continued beyond it for some distance. The outlet of Long pond, as marked in the map, did
not then exist." The channel at b being the passage for the accumulated waters of all these
ponds, was very deep and rapid, being impassable for a horse. At the same time, from near
the point a there extended a sand-bar, obliquely, into the lake, crossing the line of the channel,
and beyond it turning toward the other shore. The water on this bar was comparatively
shallow, being generally less than two feet, and never exceeding three feet. By following
the course of this, I was able to drive safely across the outlet and gain the shore on the
opposite side, which would have been impossible by any other course. . .
The following diagram of the bar and beach will serve to shew its situation:
This bar is formed by the influence of two forces: the waves washing in, which carry for-
ward the sand and deposit it in long beaches; and the opposing power of the steady current,
which neutralizes that of the waves, and the sand thus falls down in a broad curve. The
force of the current is principally expended in opposing the waves of the lake, and becoming
diffused, it flows quietly out over the bar. This continues while there is no more than ordi-
nary force in the waves; but on the occurrence of a violent northeast wind, the whole of this
bar, with perhaps ten times as great an amount of matter, is driven upon the beach, closing
the outlet. This remains so long as the wind continues, but as soon as it subsides, and the
water in the ponds is able to force a passage through the beach, the old order of things is
resumed, to be again subverted and again renewed. Such, simply, is the operation of one
stream, as it has existed for the last four or five years; and such would be the history of
hundreds of large and small streams along the lake shore.f * - -
* This map is copied from Burr's county maps, published in 1829, which was probably correct at that time.
ł By comparing this sandbar with the illustration page 350, we find that it bears the same relation to the beach that the “little
ridge” does to the main ridge. If we suppose the Niagara to have been flowing into the lake at the period when it stood at the
elevation of the Ridge road, may not the little ridge have been a bar, formed in the same manner as this miniature representation,
by the opposing force of the river current and the advancing waves of the lake º That ridge, several miles in extent, bears no
greater proportion to the power of the stream than does this insignificant sandbar to the outlet of these ponds. In reasoning a
priori, we should infer that the beach would be destroyed under such circumstances; but such is not true, in fact, as we see by
this instance and numerous others. These ridges are not always curved so much as represented in the drawing, and are often
nearly parallel with the beach.
LAKE RIDGES. - 357
What a chapter does this simple process open in the former history of our great lakes, or
in the present history of these and of the ocean where large rivers are flowing in How many
bars of sand and mud may be thrown down at the mouths of rivers which are beyond the
reach of waves, and which only become known when the coast is elevated | By the gradual
and constant rising of a portion of the continent, a series of such ridges may be formed, each
of which will be at a lower level than the preceding one, and which, when the whole is ele-
vated, would present an interesting series of parallel roads and ridges, as we may see to some
extent in the ancient lake ridge, and along the present lake shore. May it not be possible
that some of those ridges which have been identified as ancient moraines, are ridges which
have been formed in this or a similar manner } . -
The beach before alluded to, between the lake and these ponds, is nearly a mile long before
coming to the outlet; from fifty to one hundred feet wide, and generally not more than five or
six feet above the lake. For the last few years it has been wearing away, and the roots of
large trees growing upon it are becoming exposed, and some of the trees themselves are
thrown down. - - *.. - - -
Farther westward, and along the distance between b and c (see map above), the space
between the lake and the marsh is five or six hundred feet wide. This is occupied by three
distinct ridges, running parallel with each other and with the lake. Near the western extre-
mity, these three ridges divide into four, but continue equally well marked. Their summits
are from six to eight or ten feet above the lake, and the valleys between them are from four
to six feet lower than the tops of the ridges. The materials of which they are composed are
similar to the recent lake beaches, consisting of pebbles and sand covered with a light sandy
loam. They are overgrown with large trees of oak, elm, beech and button-wood, which shows
their antiquity. Their form is distinct and well-marked, while the cause which gave rise to
them more than a hundred years since is still active, producing other similar ones before our
eyes. These associations carry us back to the time when the great ridge was washed by the
lake; when the same causes were in action over a more extended surface, to produce that
striking feature, which cannot fail to convince us of the former elevation of waters in the valley
of Lake Ontario. ----- -
I might go on to illustrate the condition of the beaches and outlets farther west, but these
few examples are applicable to the whole. The ridge or beach west of Long pond is undi-
vided, and in many places from ten to twenty feet high, showing that a variation of a few
feet in height can be no objection to the mode of formation. These ponds and marshes, which
are now only covered with Sparganium and some coarse water plants, are rapidly becoming
dry; and the process by which several are drained in one outlet, by keeping open the channel
from the greater force of water, will tend more certainly to produce the result. During the
time that these outlets remain closed, the water within the ponds is raised above the level of
the lake without, and at the same time the mud and silt is brought in and deposited upon the
bottom; by this process, we see in what manner those marshes now below the level of the
lake will be raised above it. - -
358 GEOLOGY OF THE FOURTH DISTRICT.
The closing of the outlets of some of these streams is owing to the diminished quantity of
water flowing into the lake by their channels. This arises from causes before explained, and
which are constantly operating. For many years previous to 1835, the lakes were all at a
lower elevation, and this allowed the formation of bars and beaches at the outlet of streams
which before opened by a deep channel into the lake. - “.
Some of the bays along Lake Ontario formerly admitted vessels for several miles, while at
the present time they are partially or entirely closed. The beach formed at the mouth of
Irondequoit bay has a narrow opening of three feet deep, while formerly it was a quarter of a
mile farther east, and of a depth sufficient to admit sloops which took in freights at the head
of the bay three miles distant. This bay is so situated, that it receives the abraded materials
of the banks of the lake, both from the east and west. It is one mile and a quarter wide,
gradually narrowing southward; and it is separated from the lake by a sandbar or beach from
fifty to two hundred feet wide, and rising from three to twenty feet high. The greater part
of this beach has accumulated within the last fifty years. At that distance of time, it was
very low, and scarcely covered with grass; it is now overgrown in some places with large
trees. The sand and silt brought down by the stream into this bay are gradually filling it up,
and eventually it will become a marsh, with the stream winding through it to the lake.
The Twelve-mile creek, in Niagara county, presents a somewhat similar case. After the
junction of the two branches, it runs in a deep broad channel nearly parallel to the lake shore
for some distance, and its outlet is entirely closed with a beach of sand and pebbles. When
the water accumulates so as to render the stream impassable, a channel is cut through the
beach, which, from the greater flow of water, is kept open for a few days, when it again
closes. The water in this channel, for two miles from the lake, is thirty feet deep, and ves-
sels formerly entered here and loaded at that distance from the lake. We have here a re-
petition of the same circumstances as at Irondequoit bay. The diminution in the quantity of
water has doubtless been one great reason for the closing of the outlet; for had it been
greater, the outlet would have been kept open.
These are a few of the simple operations which, some centuries hence, will leave all this
marshy region dry land, bounded by long ridges, the ancient beaches of the lake, through
which the diminished streams will have made their way as in the ancient ridge which is now
some miles distant from the lake. The same will eventually take place in all the lakes, though
the process is so slow as to be scarcely perceptible. But we are to remember that the opera-
tions of nature are the same, and the causes never cease; so that if from analogy we prove
that all this change has taken place, then by the continued existence of the same causes, we
can anticipate, in a partial degree, what is still to result where the same materials are the
subject of the experiment.
MUCK SWAMPS. - 359
CHAPTER XVI.
Muck swamps—Lake marl, and tufa or travertine—Discoloration of sands and
clays by percolating water.
The accumulations of calcareous marl and tufa or travertine, are among the most interesting
and important of the modern formations. The early condition of the surface; the existence
of large lakes, and their mode of drainage, has been before alluded to. In much more recent
periods, and within the limits of human recollection, other changes, perhaps not as extensive,
but of the same nature, have been going on. Small lakes are gradually drained by the deepen-
ing of their outlets, or filled up by the accumulation of sediment brought in by their tributaries,
The effect becomes the same in both cases: as the water grows shallow, a growth of vegeta-
tion, fitted for the condition, springs up on the bottom; the plants are at first few, but the
accumulation of mud and silt around these prepares the bottom for a stronger growth; and,
finally, it becomes covered with the marsh grasses, Sparganium and the like. Mosses and
shrubs sometimes succeed this, and finally larger trees, till the whole becomes overgrown with
forest. - - --
The luxuriant vegetation which thus year after year decays, and is accumulated upon the
bottom, forms a thick bed of muck. In the Fourth District its condition is not that of peat,
it being loose and friable, and crumbling to pieces when dry. -
Many of these muck swamps are very extensive, and of the utmost importance to the
farmer as a source of manure for his crops. In the southern counties, where vegetable ma-
nure is much needed, there are large tracts which could be drained at a moderate expense,
and which would prove an invaluable acquisition to the inhabitants; for not only will they
yield a constant supply of manure, but they are even more productive than the higher grounds,
which are cultivated, while these are neglected. Along the south side of the Ridge road, and
upon the borders of Lake Ontario, there are also extensive swamps and marshes, which, even
in the natural course of things, are becoming redeemed from this condition.
The Cayuga marshes present an area of sixty thousand acres, which are almost useless in
their present condition, but which may be reclaimed, and become some of the most valuable
tracts in Western New-York. Even the growth and destruction of vegetable matter, and the
accumulation of mud and silt, will eventually redeem this tract, though by artificial means it
would be much sooner accomplished. This immense area has once evidently been a portion
of the lake, and deeply covered with water. The outlet of Seneca lake has deposited here
360 S, GEOLOGY OF THE FOURTH DISTRICT.
the debris of the strata it passes through, as well as much that has been brought in by other
sources. The consequence has been a gradual filling up of the lake, until vegetation has
taken root upon the bottom, and produced by its decomposition the extensive deposit of muck
which covers the whole. There are similar deposits at the head of all these lakes, and in
some cases considerable tracts have been reclaimed.
\
Lake Marl and Tufa.
In nearly all situations the muck swamps are underlaid by a deposit of calcareous marl.
This is usually very finely pulverulent, and, though cohering when wet, is very friable when
dry. When this calcareous deposit is made upon the surface, or in situations exposed to the
air, it becomes a tufa or travertine, often preserving, in a most beautiful manner, the impres-
sions of twigs and leaves, etc., so perfect that the species may be determined. -
This marl is derived from two sources, one being the limestone rocks themselves, and the
other the calcareous particles distributed through the superficial detritus, the origin of which
is still the limestone formations. The drift materials being composed, in a large proportion,
of the debris of the rocks of the district, calcareous matter is widely diffused. This is not
only a constant fertilizing agent in the soil, but, from the action of rains upon the surface, and
the passage of the water through these superficial deposits, the calcareous matter is dissolved
and carried forward into some lower situations, where it accumulates in the bottom of the
small lakes and marshes. By this process, extensive beds of marl are formed in portions of
the district remote from any limestone formation of the older rocks. These deposits occur in
the southern counties, wherever the drift from the northern part of the district has accumulated.
In situations above the reach of this influence, the soil has too little calcareous matter to pro-
duce any such deposits, and consequently the elevated swamps in the southern counties are
mostly destitute of it. This, however, is not universally the case; for the bed of Casadaga
lake, and the marshes around it, contain deposits of marl. -
Some of the most extensive formations of this kind in the district are made upon the Onon-
daga Salt group, and are deposited from the copious springs which rise along its southern
margin. By referring to the head of Springs, under Corniferous limestone, it will be seen
that there is a large surface drained through the fissures of that rock, and that this water flows
out in the form of springs, on the north side of the terrace formed by it. -
These deposits of marl usually rest upon a bed of clay or sand, and are succeeded by muck.
In the greater number of localities its formation has long since come to an end, but in others
it is still in progress. In many of the springs issuing from the rocks, its daily deposition can
be observed; it incrusts all the vegetables growing in the stream, and, in favorable situations,
forms deposits of considerable extent. The tufa is used for building stone; being soft, when
first removed from its bed, it is easily cut, or hewn into blocks of convenient size. These,
after drying, become comparatively hard, and form a durable material. There are, however,
but few situations where there is a quantity sufficient to allow of its being used in this manner.
MARL AND TUFA. 361
In the bottoms of all the lakes in the northern and middle parts of the district, the Chara
abounds, as it also does in the beds of streams, where the water is charged with calcareous
matter. By dredging along the bottom, it may be brought up in large quantities, and the same
takes place after high winds. The prevalence of a high south wind is sufficient to strew the
shores of Seneca and Cayuga lakes with this vegetable. It is always incrusted with, indeed
apparently almost changed to, carbonate of lime. It is at first green, but by exposure soon
becomes white, and crumbles to powder in the hand. -
In the outlet of the Caledonia spring this vegetable grows so rapidly, and so abundantly,
that it chokes up the mill-races, and requires to be constantly removed. The presence of
carbonate of lime seems favorable to its growth ; for in other similar situations, where this is
absent, it does not flourish. -
In the greater number of the marl beds the remains of fluviatile testacea are very abundant,
though it is only in a few situations where they have formed any large proportion of the de-
posit. The shells appear to have flourished in immense numbers, probably from the facility
with which they obtained calcareous matter, and other favorable circumstances; but still it is
plain that the formations of this kind are generally due to calcareous springs, or to the perco-
lation of rain water through the surrounding rocks, which, from its excess of carbonic acid,
dissolves the calcareous particles in the soil or the harder strata. .
The shells occurring in these deposits are all of recent species, and indeed the same may
often be found, still living, in great numbers, in the marshes above the marl. The Limnea
jugularis, Planorbis bicarinata and two or three other species, Valvata tricarinata, and
Cyclas similis, are among the most abundant species. f -
“. . . .
Discoloration of sands and clays from the percolation of water.
The discoloration of sand and clay beneath muck swamps, or vegetable deposits of any
kind, is deserving of notice as sometimes leading to important conclusions. The green lines
and patches in the Medina sandstone have been attributed to the deoxidation of the iron, from
the presence of carbonaceous matter. The same is noticed in the Old and New red sand-
stones, and indeed in all rocks colored by oxide of iron. In the superficial deposits, the pre-
sence of free carbonic acid renders the water capable of dissolving and removing the coloring
matter, forming deposits of the hydrous peroxide of iron. This takes place with great facility
in muck swamps, or where there is a deposit of vegetable matter above the soil. In this way
we are to account for the white gravel and sand found in Swamps and bog meadows. In some
cases the change is only partial, and in others there seems a change from a lower to a higher
state of oxidation.
We usually find two kinds of clay noticed; the blue and yellow, the latter succeeding the
former, and generally supposed to be a subsequent deposition. This may perhaps be true in
many localities; but in Western New-York, not only the clays, but the other superficial de-
posits often take their color from the effect of the percolation of water, which probably changes
the state of oxidation in the coloring matter. The surface deposits have originally been of the
[GEOL. 4th DIST.] 46
362 GEOLOGY OF THE FOURTH DISTRICT,
same blue color as those beneath, and this change takes place after sufficient exposure. This
may be made apparent by the following illustration :
#
:=
i
E:===
§§
#
=====
---
º->>-
-º-º:
Sº
E-St.
-
:*-*
º:-
º:-->
ES:s:SE is:=
*-*-*. º:SE
*- sº :-->
Eº:===s: #=
=E, --~~~~-- :E==
fºss---º--- 'E:-->
E= *~ •-------
> SES-> Z===
E=3 -S-S-AS-S-> $E .
* -- -º-º-º:
E= :S→S-> *-*
ES-25E ESE --~~~-ºs.
Eas: Eğ:SãSEEs==<= *>
Peº:=:: *Sºrrºr--> --~------
- £º --> ***
- Eºs::S→S: sº->-> ºfflº-E
-->= --> --~~~~- >>
F:S: E *- *-*= ----------
--~-
===#v==\; ºs::=ES FS-S-S-S-E .
E. w
===s= Se:S→S.--> -
E EEBSE:F. Fºs::s:S→Se:S3; sº tº:5:-
E:SE: EP Eºs::s:sº º º:S→7
E= ==E:s ====E=SES 3:----> ºs:==F g
E::=EEE ES:S→SESES: :ET
E: EEES-E:S→ º:-
E EAESES: Si:S→S:S→S:S:SE º:=>"
- E- ->>~ ET
*EiE: ES:Sºs::s:S→Sºrºs.:S:S→S3 Es==
s S-S->\º.
AE Eºs::s:=SE<\e:
Yºº-º-º-º:
::=s== &:
---
-
Bank of blue and yellow clay, Dunkirk, Chautauque county.
The lower deposit is a blue clay, with small pebbles or gravel sparingly intermixed; the
upper part is a yellowish brown clay, with veins of the same penetrating the blue clay in the
manner represented in the woodcut. The upper part is distinctly mingled with gravel, as
well as the veins, while the blue appears a more pure clay; but this appearance is fallacious,
for on examining the blue portion, it is found to resemble the upper precisely, except in color.
Farther examination also proves that these veins are merely apparent, being caused by the
discoloration of the blue clay from the percolation of water. The water sometimes penetrates
laterally, and produces beautiful ramifications of the yellowish veins. In this example the
process is perceptible, and the passage of water along these lines can be witnessed at any
time. In many other cases the cause is not so apparent, though in a large number of instances
I have been able to detect the same agency, attended with similar results. -
This is a subject well worthy of attention, not only among superficial deposits, but among
the older rocks; for these have often been near the surface or above water before their in-
duration. How far it may explain the change or alteration of color in successive strata, or
the apparent veins of segregation in some of our rocks, I am not now prepared to decide; but
I have seen numerous examples apparently due to changes of this kind, which have operated
before the strata became fully consolidated.
In the clays, it of course happens that the yellowish deposits are subsequent to the blue,
and they are often more pervious to water from an intermixture of sand; but the limit of the
change in color will be found at the depth to which surface water penetrates. The lower
clays are the more purely argillaceous, and therefore less pervious to water; consequently
this portion of the deposit retains its color, while the more sandy parts are rapidly changed.
FOSSIL BONES OF QUADRUPEDS, 363
173.
w - * - º -
t! º,..., " ' -- mºst
* . ~~~~
| | º *-*
iſiſ,
ºf a
º º º
||ftº/
\||º/
\ll; ºf | º º
|
ſº
... . . . . . . . . ;
ºr . . . wºn.
Niš. º §
§yº
º * §: sº \\ {{
\\
s
| W: fº WN WA Wilkillſº it. W \\ \\ Mºſſ ſº | § § ſº : . ſ
º º º
º º V Wºº * {
: ſº 2. º | Wºº \\ \º º
|####||||||| tº ſºliº \\ \\ºj|| || ||
º º | \º º º
º º | º
|||}|...}} \\ tº \\ºº
º º | º
º/ Vº tºº. º
% tº \!\!\!...ºft. º º:
º
§
|
.
\ * * º
º º
t
\
§
| |
t!
º
i.
|
§
ºś. \ \
º Ç ſ
"… " \\ tú t ń.
W.
\\ \ | º
\ \; \ º º
\\\\\\\ º *W º |
\ wº º § wº
\
\
\
\
\\ #) \\ (W. | jº
\'ſ \{i};
- § - Ú
§§ r
Molar tooth of Mastodon maſcimus. Geneseo, Livingston county.
CHAPTER XVII.
Fossil Bones of Quadrupeds.
Fossil bones of the Mastodon have been found in numerous localities throughout the dis-
trict, and, since the relative period of their existence is one of much interest, it seems desira-
ble to ascertain the comparative date of the formation in which they are imbedded. These
remains are not only distributed throughout the Fourth District, but have been found in all
that part of the State west of the Hudson river and south of the valley of the Mohawk. But
46*
364 GEOLOGY OF THE FOURTH DISTRICT.
two localities have been noticed on the east side of the Hudson, within New-York. In New-
England the remains of this animal are comparatively rare, and their occurrence has been
recorded in only a few localities." This rarity, when contrasted with the numerous localities
in Western New-York, and the still greater number in the Western States, shows that the
animal found a more congenial condition of the surface, or climate, at the west than among
the primary regions of New-England and New-York.
The following are the localities which have been recorded, or have fallen under my own
observation within the Fourth District : | -
1. In the town of Perrinton, in the bank of a small stream, in gravel and sand. A tusk and
several teeth were found at this place, which are now in the Rochester Museum.
2. In 1817, some remains were found in Rochester, in a hollow or water course.f
3. In 1838, during the excavation of the Genesee Valley canal, at its junction with Sophia-
street in the city of Rochester, a tusk, some bones of the head, several ribs, parts of two
vertebræ, and some portion of the pelvis were found, intermingled with gravel and covered by
clay and loam, and above these a deposit of shell marl. These bones are now in the State
Collection. The tusk is said to have been nine feet long, but was nearly destroyed by the
workmen before removing it from the clay. A portion of a tibia was also found, which is in
the Rochester Museum. - - .
4. During the excavation of the Erie canal at Holley in Orleans county, a large molar tooth
was found in a swamp near the village.;
5. A molar tooth was found in digging a mill-race at Niagara falls, several feet below the
surface. The deposit in which it occurs is a fine gravel and loam containing fresh-water
shells, and is evidently a fluviatile deposit. -
6. In a small muck swamp in Stafford, Genesee county, a small molar tooth was found
several years since. Its situation was beneath the muck, and upon a deposit of clay and sand.
A large quantity of hair-like confervae, of a dun brown color, occurs in this locality; and so
much does it resemble hair, that a close examination is required to satisfy one's self of its
true nature.” -
7. In 1841, a molar tooth, weighing two pounds, was found in a bed of marl three miles
south of Le Roy.
8. At Geneseo in Livingston county, several years since, a large number of bones and
three teeth were found in a swamp beneath a deposit of muck, intermingled with a sandy
calcareous marl. A single tooth, in the possession of C. H. Bryan, Esq. of Geneseo, is the
only known remaining specimen of this collection. The figure at the head of the chapter is
from this fossil.
9. At Hinsdale, Cattaraugus county, a tusk, with some horns of deer, were found sixteen
feet beneath the surface, in gravel and sand.
* See Hitchcock's Geological Report, page 402. + See New-York Fauna, Vol. 1, Part 1, p. 103.
f For this information I am indebted to Col. Elisha Johnson of Rochester, having seen no published notice of it.
FOSSIL BONES OF QUADRUPEDS. 365
10. At Jamestown, Chautauque county, a tooth of a mastodon was found several feet
beneath the surface, in gravel. Dr. Emmons has in his possession a tooth from the same
neighborhood, said to have been found in a bank of clay. Dr. De Kay refers this specimen
to the American Stag. .*
The localities enumerated are all that are known as occurring in the Fourth District. The
different positions in which these remains are said to have been found, will probably all admit
of one explanation. - -
Notwithstanding the numerous localities which have been examined, and the great numbers
of bones disinterred, there still seems to exist among many a doubt as to the period of their
existence upon the earth. Their bones are said to be found in the diluvial or drift, thus
identifying them with that period which, from all testimony, seems to have been one of general
submergence beneath an ocean, and we have no knowledge of a previous condition of the
surface fitted for their existence. It is doubtless true that these bones often occur imbedded
in gravel and sand of the nature of the ordinary drift ; but in such instances it can usually be
shown that they have been transported, and that the deposit in which they occur is one of very
modern origin. - - - .
In all situations where these remains appear to have been left undisturbed, they are asso-
ciated with the most recent deposits, proving that the animal has existed upon the surface
since the present condition of things prevailed. - - -
In speaking of this subject, Dr. De Kay remarks, that “The geological period at which
this huge animal existed, has occasioned much attention. It must have been among the most
recently extinct of all quadrupeds, unless we except some species whose generic types still
exist on this continent. Rejecting as altogether fabulous the pretended discovery of the
stomach of this animal, with its contents, consisting of reeds, twigs and grass, as detailed by
Barton (Med. and Phys. Jour., Vol 3, p. 23), it has certainly been discovered in positions
indicating that the animal perished and left its bones on or near the surface where they are
now found. Cuvier states that the mastodons discovered near the Great Osage river were
almost all found in a vertical position, as if the animals had merely sunk in the mud (Oss.
Foss., Ed. alt. Vol. 1, pp. 217, 222). Since that time, many others have been found in
swamps, a short distance beneath the surface, (frequently some of the bones appearing above
the soil,) in an erect position; conveying the perfect impression that the animal (probably in
search of its food) had wandered into a swamp, and unable to extricate himself, had died on
the spot. Such an incident doubtless occurred to the animal whose remains we assisted to
disinter, some years ago, at Long Branch, New-Jersey. He was in a natural vertical posi-
tion, his body supported by the turf soil or black earth, and his feet resting upon a gravelly
bottom. The occurrence of the bones of other animals not yet extinct, in company with those
of the mastodon, is not a conclusive evidence of their contemporaneous existence ; but we
cannot deny that it furnishes strong reasons for believing them to have been of a very recent
date. We think it highly probable that the mastodon was alive in this country at a period
366 GEOLOGY OF THE FOURTH DISTRICT.
when its surface was not materially different from its actual state, and that he may have
existed cotemporaneously with man.” - - -
Of the very recent existence of this animal, there can be no doubt; the marl beds and muck
swamps where these remains occur are the most recent of all superficial accumulations (in-
deed they are now forming), and the surface had arrived at its present condition generally
before these began to be formed. Any great change, such as the submergence of the land,
would obliterate these deposits, and mingle their contents with the surrounding drift. That
they are of very recent formation, is also proved from their usually resting on the drift, being
the latest deposits in shallow lakes after the final deposition of the sand and clay and the
elevation of the continent. - - -
The situation of the bones in the Fourth District offers no exception to the general rule, but
rather confirms it in all instances. In the first named locality in Perrinton, the deposit of
gravel and sand is a recent one, made by the stream on which it occurs. -
In the third instance, the bones were somewhat mingled with pebbles, and a portion were
lying against the side of a large boulder; but the deposit covering them was evidently of very
modern origin, containing fluviatile shells. The surface for some distance around had evi-
dently been a lake, which was subsequently filled up, and became a swamp; and finally,
since the settlement of the country, this swamp has been reclaimed. º
In the fourth instance, the tooth was in the bottom of a muck deposit, and above the gravel.
At Niagara falls the deposit is a very modern one, containing shells of recent species, and
evidently of the same age as Goat island, which is elsewhere described. The tooth was pro-
bably drifted by the current into the situation in which it was found, and therefore furnishes
no knowledge of the period of its existence, but proves the deposition at that place to have
been subsequent to the destruction of the mastodon.
The specimen at Stafford, in the bottom of a muck swamp, was probably part of the re-
mains of an animal which had perished here, and had never suffered transportation.
In the case at Geneseo, where the bones were said to be imbedded in gravel, it is proved
to have been a shell marl.f -
The deposit of gravel and sand in which the remains of mastodon and deer were found in
Cattaraugus county, is one of very recent origin, having been made from the ruins of the drift,
by the stream along which it occurs. --> - -
The same is doubtless true of the formation at Jamestown, as there are some extensive
deposits of recent origin at the outlet of Chautauque lake; but I have not examined this
locality. -
It appears, therefore, from a consideration of all the facts, that the apparent instances of
* New-York Fauna, Vol. 1, Part 1, p. 105.
# While Mr. Lyell was in this part of the country, being desirous to ascertain the truth among conflicting statements, he pro-
cured an excavation to be made at the spot where the bones were originally found. Some fragments of bones were obtained,
mixed with marl and freshwater shells, leaving no doubt of the position of the animal, which doubtless perished on the spot where
these remains occur.
FossIL BONES OF QUADRUPEDs. 367
bones imbedded in drift are accounted for upon other principles, at least so far as regards the
western part of New-York. The most probable explanation appears to be, that a marl lake
has been suddenly drained, and its contents, mixed with gravel, sand and boulders, transported
to a distance, where the whole was left as a deposit resembling the ordinary drift.
I might mention two other localities which I have visited; one at Coeymans, and the other
at Greenville in Greene county, where the bones were imbedded in a freshwater marl, or
rested upon the clay beneath the marl. There is here no possibility of their having been
transported; and the inference of Dr. De Kay, that these animals perished while in search
of food in swamps, seems substantiated by the position of their bones.
It has been noticed as a remarkable fact, that the bones of other animals have rarely been
found with those of the mastodon; and of this, the circumstances just mentioned may perhaps
offer some explanation. If the nature of the animal induced it to search for food in such
situations as we find their bones, those that sunk in the mud, or died there, would be pre-
served; while other animals, having no inducement to go into those places, would leave no
evidence of their existence. The bones of other animals, and even those of the mastodon,
when left in situations exposed to atmospheric influences, and as a prey to smaller gnawing
animals, would be destroyed, and no vestige of them would remain. This we know to be
true, from the fact that although the country has been long inhabited by great numbers of
moose, deer, bears, wolves, and a variety of smaller animals, yet rarely any of their remains
are found; it is only in situations favorable to their preservation that they occur; and the
same is true of the mastodon. It thus appears probable that the remains of this animal which
we find are but a moiety of the hundreds and perhaps thousands which died in other situa-
tions, and left no record of their existence.” - -
From all the facts observed, it seems not very improbable that the mastodon has lived since
the continent was inhabited by man. In the earlier condition of the surface, it was probably
better fitted to sustain these animals; the kinds of food they required grew more abundantly,
the nature of the surface was adapted to their habits. Subsequently this state of things be-
came changed, and small portions only may have afforded them the required kind of nourish-
ment; under these circumstances they have become extinct; not suddenly, as has sometimes
been conjectured, but gradually as the conditions of the surface became incompatible with
their existence. In this respect doubtless their mode of extermination resembled that of some
other animals which have disappeared, and are disappearing from the earth. In the latter, the
influence of man has had a large share in the process; while in the former, we are not aware
of any such influence, unless we give credit to the aboriginal traditions. -
* Mr. Williams, one of the assistant engineers, has informed me, that at the summit level of the Genesee Valley canal near
New-Hudson, four miles from Cuba, several deer's horns and the horn of an elk were found twelve feet below the surface, in a
muck deposit. In the same situation, a piece of wood, gnawed by beavers, was also found. These are all remains of existing
animals, but the position is the same as that in which the bones of the mastodon are found.
368 GEOLOGY OF THE FOURTH DISTRICT.
- *:... :-º"...: '… - -*-se&*. 3:..."~...~~. -
-- --------...--------→s*-ºs------. §§ -
- ---- ----- --º-º-º: sº-ººs::s ===s=- - --
_--———- #:#;===######s==
Tº =#E=s===
====E-
*-m-m-m--- - - -
º
§ --> |####
º
º |;
iº
º ğ gº
º
\\\
sº
§§
§
º
Ş s §º §
§§§º §
Lower falls at Portage, from the west bank of the river. From a sketch by Mrs. HALL.
CHAPTER XVIII.
Modern action of rivers—Freezing of water in river channels.
The numerous examples which we have in the Fourth District, of rivers flowing in deep
narrow gorges, naturally prompts the inquiry whether the present streams can have formed
the channels in which they now flow ! Fully to answer this question, would lead to the con-
sideration of numerous circumstances, and open a wide field of inquiry. Every river and
smaller stream, even the most insignificant, will furnish facts for illustrating the subject.
Although we may find these modern operations upon a much smaller scale than in the moun-
tainous regions of Northern New-York, still the effects are everywhere visible. The trees
standing upon the very margin of a stream falling over a rocky stratum, or upon the edge of
a cliff with their roots projecting more than half over the precipice, or even the tree itself
prostrated and held suspended only by a few fibres which penetrate the soil beyond the chasm,
are eloquent monuments of the changes wrought by time upon the rocky cliffs and deep river
gorges. These show that nature in all her operations is constant and unremitting, and that the
MODERN ACTION OF RIVERS. 369
least perceptible change within the memory of man becomes a vast incomprehensible amount
during the millions of ages through which the earth has arrived at its present condition. If
a river channel can be widened and deepened to the amount of a few inches within the recol-
lection of any individual, may not a gorge of one or two hundred feet be formed by the same
process? Our theories of modern operations make provision for wide sweeping deluges, for
immense excavating waves, for hemispheres of ice, the upheaval of mountain chains, and the
transportation of ice floes from frozen islands in our own latitudes; but we have almost for-
gotten the quiet operation of running streams, and the freezing of water in fissures of hardened
rocks. * . - -
In the first place we may consider a few of these effects which are known to us, and after-
wards compare them with similar ones which may have resulted from the same causes. By
this method we shall be able to prove that rivers have worn their channels not only through
preexisting beds of modern detritus, but also through the barriers of solid rocks.
The sketch at the head of the chapter represents the lower falls of the Genesee at Portage.
The bed of the stream is bounded on either side by cliffs three hundred feet high. Upon the
left bank is a table of rock, which was formerly the river bed; and upon the right is a small
conical island of rock, between which and the table on the other side, the stream now flows.
Within the memory of the oldest observers, the river flowed almost wholly over this table
rock, and the isolated mass was joined with the right bank of the river. The following dia-
gram will enable the reader fully to comprehend its present and former condition : -
175,
*- t - - - - A.
A, B, represents the width of the chasm at the top. - •.
a, a. The platform or bed of the stream, over which the water was originally precipitated ninety six feet to the level of the
river below the falls. This platform a a was formerly continuous to a'. -
b. The narrow channel of recent excavation. , A
d, d, and c. A recert gorge, separating the small island from the main bank.
[GEOL. 4th DIST.] - 47
370 GEOLOGY OF THE FOURTH DISTRICT.
This table or platform is composed of a firm sandstone less than two feet thick, resting on
softer strata beneath. A slight depression had been worn between a and a', over which a
larger portion of water flowed than over the space between a and a. This depression in-
creased in depth by the wearing action of the water and the effects of freezing, so that long
since, the great body of water has flowed through this recent channel. During freshets, and
at the breaking up of the ice in the spring, the narrow channel on the right is filled, and it
then flows over the table above to the depth of a few inches. - -
The following ground plan of the river at this place will illustrate its condition at the period
before the projecting mass of rock was worn through Yº -
f
a, a. The table or platform, which originally extended
across the whole width of the river's bed. . .
d, d. An elevated projecting mass of rock, standing in
the direct course of the current. -
The first operation by which this change was effected, seems to have been a deflection of the
current to the right side, caused by a bend in the river above. This force diminished towards
the edge of the fall, and the projecting portion of the cliff d, d, was thus protected for a long
time, until the channel on the right side, becoming deepened, drew off nearly all the water in
that direction, when it was gradually worn through. When first known, this isolated mass
was joined to the main cliff; and when subsequently a passage was formed at c, the upper
part still remained connected with it. This arch was afterwards broken down by the action
of freezing water and its own weight, leaving it in its present condition.
The principal modern effect illustrated in this example, is the formation of the narrow
channel on the eastern side of the river bed, which now extends back from the fall about one-
eighth of a mile, being in its greatest depth about eighty feet, and nearly the same in width.
For the whole of this distance it forms a violent rapid, and the action of water and ice is con-
MoDERN ACTION OF RIVERS. 371
stantly tending to increase its dimensions. Within five years, the period of my own observa-
tion, it has been deepened in some places five or six feet, and its southern termination has
extended several rods. Except during freshets, or the breaking up of winter, the water does
not flow through the channel c of diagram No. 175, and consequently the wearing action has
nearly ceased in that direction. The stream, however, is directed against the little island
seen in the sketch, and will eventually remove it, making for itself a direct channel to the
gorge below.” - ... . . -
If all the changes here described have taken place within the last forty years—if a river of
the power of the Genesee has in one place excavated a channel of these dimensions—what
results may we not ascribe to similar action in larger bodies of water It is not too much to
say that the deep gorge from Portage to Mount-Morris has been worn in the same way, or
that the chasm of Niagara, from the falls to Lewiston, has been excavated by the stream now
flowing in its bed. In making these estimates we are not to count time by years, but by
ages; and there is abundant testimony that years beyond our comprehension have passed
since the surface of the earth assumed its present form, and since the rivers began to flow in
their present courses.
I have cited this case as an example, because it is one well known, and where observations
have been repeatedly made; and because, within the last five years, I have examined it seve-
ral times, and each time with a conviction of the changes that were in progress. The break-
ing up of the ice every spring removes large masses of rock at the head of this channel, and
these, with others, are carried forward through the gorge, with a force that tears up its bed
and sides. The table above, which was formerly the bed of the river, will, in a few years,
become covered with soil and vegetation; strong grass and willows have taken root in the
fissures, and these collecting about them a little earth, giving a soil for the support of the
other plants, the evidences of its original condition will be lost. A century hence some incredu-
lous observer may stand on the edge of this table rock, then covered with shrubs and trees,
and deny that the insignificant stream flowing in its bed can have excavated this deep chasm.
An observer of similar dispositions may now stand upon the margin of the great gorge of the
Genesee at Portage, and say that it is impossible for this river to have worn it to the depth of
three hundred and fifty feet, and with a breadth of six hundred feet. But the Genesee was
once a more powerful stream, and it has flowed in its present direction longer than we are
usually accustomed to consider as the age of the world. - . .
The consideration of this small portion of the channel of the Genesee leads us to the exami-
nation of the whole of that deep gorge extending from Portage to Mount-Morris. The greater
portion of the channel for this distance, so different from that in which the river flows, either
to the north or south, requires a different explanation of the mode of its formation. The river
flowing northward from its source through the valley south of Portage, then bends around to the
* For a knowledge of the early condition of this fall, and many of its successive changes, I am indebted to my friend Colonel
Johnson of Hornby Lodge, who explored this part of the country in 1808. Col. Williams, an early settler in this region, gave
me a very similar account of its condition when first known to him.
47%
372 GEOLOGY OF THE FOURTH DISTRICT,
left, and pursuing, for a short distance, an almost opposite direction, again gradually assumes
a northerly course; but here, instead of the alluvial bottom of a broad valley, with sloping
sides, it flows through a deep narrow gorge, and in the space of less than two miles pre-
cipitates itself over three falls, descending about four hundred feet.
It is to be recollected that in all the narrow portions of this gorge the cliffs are nearly or
quite perpendicular, the chasm is narrow, and there is no deposition of drift or alluvium in
its bottom. The bed of the stream presents a vast accumulation of fragments, fallen from
the sides of the chasm, and there are few or no rocks of foreign origin. From the very
aspect of this kind of channel, when compared with the broad deep valleys, we would at
once decide, that it is of more recent Origin. - - -
In examining the country north of Portage, in the direction of the river, on the south, we
find a valley filled with an accumulation of sand and gravel. This has been sounded, in many
places, to such a depth, and over an extent so great as to authorize the conclusion that it was
an ancient valley which received these deposits. The uppermost of these is very modern, as
was before shown (page 345), and doubtless made after the river was formed; indeed, proba-
bly after it had followed this channel for some length of time. The inundation of gravel and
sand closed this former valley, and the Genesee on the south became a lake. It then took a
course westward, over the lowest barrier, which appears to have been in the direction of its
present course Here it has formed for itself a channel in the rocky strata, worn in some
places to the depth of three hundred and fifty feet. -
The following diagram shows the respective positions of the ancient valley, now filled, and
the present river channel : - -
177, ,
a. Present channel of the Genesee.
c. Ancient channel, filled with modern detritus.
b. Strata of shale and sandstone of Portage group,
MODERN ACTION OF RIVERS. 373
Whatever may have been the causes which closed the old channel, there can remain no
doubt of the mode in which the new one was formed. We can think of no other cause than
the action of the stream itself, that would excavate such a channel, with vertical walls, and in
a direction so devious. If it were of the age, and formed by the same means as the majority
of valleys, it would be broader in proportion to its depth, and its sides and bottom present
some deposits of drift. Where the stream emerges into an old valley on the north, near
Rogers' bridge, after making this circuit, a distance one-third as great, direct from Portage,
would have brought the stream through the old valley filled with drift. Between Rogers'
bridge and St. Helena the direct route is filled with drift, while the river channel is a narrow
deep gorge, making a circuit of three miles. Again, for three miles before reaching Mount-
Morris, the same devious course is pursued, and the banks are almost equally precipitous,
though, from being shales, they are less abrupt. In all these instances the banks bear the
marks of a freshness of excavation not to be mistaken. It is emphatically a modern channel.
178.
The accompanying illustration represents the course of the
river from Portage to St. Helena; a direct line between the
two places would have passed in an ancient valley, while all
the deviations are through rocky strata, and in deep gorges.
a. Position of the lower falls of Portage. -
This example is sufficient to enable us to understand how a river, when obstructed in one
direction, will excavate a channel in another; and even, though the obstruction be only loose
materials, it often finds an easier course by wearing down hard rocks than by removing gravel
and sand; making a circuitous route through solid strata, while a more direct one would
have been through a superficial deposit.
Nearly every stream flowing from the south, over strata of this age, presents the same
features, in a greater or less degree. A hundred examples can be cited where there is
374 GEOLOGY OF THE FOURTH DISTRICT.
demonstrative proof of the recent effects of streams upon their beds; examples such as will
make us hesitate before we decide that such effects as deep gorges can not be formed by
running streams. - -
The few lateral streams that flow into the Genesee, in its course through these gorges,
give evidence of the same recent origin in the channel. The streams either fall over the
vertical edge of the cliff, having worn it back to some little extent; or they come in through
lateral channels, with vertical sides, scarcely disturbing the continuity of the cliff, any IQ OT6.
than if a deep cutting had been excavated by artificial means. The appearance of both the
main channel and the lateral one, respectively attest their modern origin.
179.
% º
º º º .
§ %§ 5 *
%
%
ſ # º
| § sº.
wº
:=
º
... •
... •
º -
sº ºf Ež22\\\--"
- sesse T-2 £e \-=. &=
Entrance of Wolf creek into the Genesee above St. Helena. From a sketch by Mr. E. N. HoRSFORD.
The entrance of Wolf creek into the Genesee offers a good example in point. The lateral
channel is, at its entrance, a square cut gorge of nearly two hundred feet deep. Farther from
the river, however, the stream appears to have flowed in the bottom of an ancient shallow
valley, before it excavated the present gorge. Such is doubtless the fact in other instances,
where there has been a sufficient depression upon the surface to give direction to the water,
after which it has cut its own channel far into the strata beneath.
MODERN ACTION OF RIVERS. 375
Action of freezing water in deepening river channels.
The manner in which streams deepen their channels, particularly in the rocks of the southern
counties, is illustrated at every step. The rocks, consisting of alternations of hard and soft
materials, are readily influenced by the freezing of water; and the bed of any stream can
scarcely be examined, but the strata will be found elevated in the centre, and dipping toward
each side. Sometimes the elevation is on one side, and the dip towards the other. This
takes place by the water first finding its way through a fissure beneath the stratum, where it
freezes and elevates the rock; loose earth and pebbles find their way into this enlarged fis-
sure, and beneath the stratum; during the succeeding winter, a larger quantity of water
freezes beneath it, and elevates it still more. If the breaking up in spring does not remove
it, the next winter will be sufficient, and then the whole is carried onward, with ice, stumps,
trunks of trees, etc., till it finds some level place in the bed of the stream, where the whole
rests for a period, to have the same operations renewed. ... • - -
The following illustration is a sketch from the bed of the south branch of the Cattaraugus
creek. A thick stratum has been elevated by the freezing of the water, till its edges are above
the surface. This sketch was taken two years since, and probably the whole is now replaced
by others.
*-* --
=_---
=------
---
-----
* --º
---
sº
-->:sº
*-----
§:S:
G- º:
---wº- ZººZ
E->
F-------
- - -- ºff ºffſ: sº : - —==-aº -
§:::::::$# - §§ (ſ §§§ E=====
É peº:- =====::::::=EE:º:====
assºs::s:º-E TE=== I.--—— -
º Sºº E--------------------
------as- - - -
This mode of operation is constant; and no sooner is one portion removed, than another is
lifted up, to follow in the same manner. In the thick-bedded limestones, its effects are less
rapid; but even here the influence is perceptible, and occasionally large blocks are loosened
and carried down the stream.
376 . t GEOLOGY OF THE FOURTH DISTRICT.
Potholes—Effects of artificial dams.
These evidences of running water exist in several places in the Fourth District; but in all
that I have seen, they are near the margin of some stream, and in a situation easily accounted
for by supposing the water at a higher elevation. In the rapids at Rochester, small potholes
are formed in the limestone, and also in the sandstone and shales of Portage on the same
river. In the bed of the river at the Rapids above Niagara falls, large and deep potholes are
formed. These probably exist over the whole extent of the rapids, as they are visible in all
accessible places. On the western side of Goat island, there are remains of some of these in
situations higher than the water usually flows, proving therefore that the elevation is less, and
that at the time they were made, the margin of the fall was farther north than at present.
Potholes similar to these are frequently worn in rapids below artificial dams. Mr. Wilder,
of Hoosick-falls, informs me, that on turning the water to repair a dam which had been
standing twelve years, potholes of four feet in diameter, and several feet deep, were found in
the sloping rock below. Dr. Ambler, of Ogdensburgh, informs me of still more important
effects produced by the falling of water over dams. The dam at Brownville, Jefferson county,
which was erected forty or fifty years since, in a narrow place in the river, bounded by per-
pendicular walls of limestone, and flowing over a bed of the same, had a perpendicular fall of
twelve or fifteen feet. From the time of its erection till 1841, when it was carried off by a
freshet, the falling water, with all the fragments of rock, pebbles, etc. had been wearing upon
the limestone bed of the river, and had produced a cavity or pothole estimated at fifty or sixty
feet in depth. Sawmill logs of fourteen feet in length, passing over this dam, would plunge
beneath the water, disappear for a considerable time, and on coming to the surface, would rise
more than half their length above water. From this circumstance it was considered that the
depth of sixty feet was not too great an estimate. The rock is of hard grey and black lime-
stone of the Black river and Trenton limestone formations.
In another case, of the dam at Ogdensburgh on the Oswegatchie, with a fall of twelve feet,
the water has removed large slabs of limestone of a foot thick, and from ten to twenty feet
in diameter, and carried them several rods down the stream. •
Neither are these isolated instances. I could extract pages from my note books, showing
the modern effects of running and falling water, freezing, etc.; but examples enough have
already been presented. - -
WATERFALLS, 377
º
º §
#||
D º *
t º | ſº t º
d '..." n ! : g #º: §
| 5 r §illºſ
º T •
| . . . ."
º'ſ
s º
º t t -
n r
# - ; º ºº
isºlºiſ
/ º º |
º §º"|iº
º º º º:
º º º º *
* | º º . ºft
º º
§ º
º
º
§
§§ #):
ſºſ. §§ §ſ;
- - #4%Ap ~
§
ſº
Ž | º š. ºr
32.3º % #;
ºffſ,
- ſº
- º =?-A º
ºs--- ===E= ſº * .5%
- =%2::3% ºſ.
Taghan nuc falls, Tompkins county. From a sketch by Mrs. HALL.
CHAPTER XIX.
Waterfalls.
The numerous and picturesque waterfalls of the western part of the State are intimately
connected with the modern action of rivers and streams, in excavating and deepening their
channels. That every fall of water is receding by wearing back its bed, will admit of de-
monstrative proof, wherever observations have been continued for any length of time. Even
the short period of four or five years has been sufficient to show, in many instances, a constant,
gradual recession, varying with the quantity of water and the nature of the rock. The
greatest amount of water does not always, however, appear to be attended with the most rapid
recession; for where the stream is so small as to be entirely frozen during winter, the effects
[GEOL, 4th DIST.] 48
378 GEOLOGY OF THE FOURTH DISTRICT.
of ice on the strata seem even more efficient than the wearing of water. The loosening of
masses near the edge, at least, enables the water afterwards to remove them with greater
facility. -
Where we find these falls upon streams half a mile from their junction with a large lake,
it is difficult to conceive how they have once commenced their operation on its margin, and
we are readily disposed to admit any hypothesis that will account for the previous excavation
of a lateral valley to this distance from the main one. Where these channels expand rapidly
toward their outlets, and slope gradually upward, it seems a fair inference that some agency
other than the wearing of the stream has had a share in producing its present condition; but
where we find a regular chasm with perpendicular and nearly parallel sides, with a fall of
water at its extremity, we are compelled, from all analogy, to admit that the stream has been
the agent producing it. --
In the sketch at the head of the chapter, there seems originally to have been a broad shallow
depression, in which the stream commenced flowing towards the lake. In its passage, it first
produced a series of falls and rapids, but finally receded so as to form but a single fall. This
is caused by the higher strata being so much harder than those below, that a firm table is
formed of these, while those below are undermined. At the present time the fall is about a
mile from the lake shore, and one hundred and ninety feet in perpendicular height, being the
highest fall in the State. The water is precipitated into a deep chasm, with cliffs on either
side of three hundred feet in height. The stream becomes almost lost in spray before reaching
the bottom, where it is gathered in a circular pool, from which it flows over the rocky bottom
to the lake. The fall is usually approached from the lake, and it forms one of the most
romantic and picturesque scenes in the whole of Western New-York. The stream, insignifi-
cant as it appears, is nevertheless during freshets of great power, carrying forward huge slabs,
which are piled up below the fall in a manner such as we are accustomed to attribute only to
the agency of more mighty streams. -
Although there may have been originally an indentation at this point, from the valley of
Cayuga lake, yet there seems conclusive evidence that the stream has been the chief agent in
producing this immense chasm. The numerous seams freely admit the water, which during
winter is frozen, and thus from the whole face of the cliff immense quantities are detached.
In this way the upper portion is left projecting beyond the lower, till it is broken off, and falls
down. The first process is constant; and during an interval between my visits to this place,
I observed that a mass of fragments, scarcely less than fifty tons, had fallen down. This is
doubtless but a small part of what is annually separated by freezing water, and the more quiet
operation of moisture and air during the milder season.*
# The lower of the two more prominent arenaceous strata, about half way up the cliff, is the one presenting the fine casts of
striae, alluded to in the description of these under Portage group. Beautiful specimens may be obtained at this place after the
falling of a mass, or by approaching the stratum at some accessible point. Many of the strata in the channel of the stream above
the fall present these casts in great perfection.
WATERFALLS.' & 379
This mode of operation will explain the cause of recession in a great number of instances.
Where, however, the water is in such quantity as to preserve a temperature above freezing,
as in the outlets of some of the lakes, the recession is slower; the chief agents in effecting the
destruction of the rock being the wearing action of water, and the effects of air and moisture.
It may be natural to suppose, that if these streams commenced their operation at the same
period, and upon similar rocks, that they would have worn back the strata to the same distance.
The fact, however, is, that the falls are at extremely unequal distances from the main valleys
into which they flow. This may, in part at least, be accounted for from the circumstances of
a different proportion of water and a greater or less height of fall, as well also as many other
minor causes which may have operated to vary the amount of recession. Along the Seneca
and Cayuga lakes there are many examples of falls over the same strata, at almost equal dis-
tances from the lake. About one mile north of the Taghannuc falls, there is another fall of
water over somewhat similar strata; but here are no indestructible layers near the summit to
act as a table rock, and the whole elevation is worn down in a continuous slope, with some
narrow projections formed by thin arenaceous strata. Had there been, near the top, a thick
stratum, capable of sustaining the water, we might have had a fall similar to the one in the
illustration.
182 o
48*
380 GEOILOGY OF THE FOURTH DISTRICT.
Where there are frequent alternations of argillaceous and arenaceous strata, a series of
falls and rapids are produced; but, in such cases, the total amount of wearing action is far
less. The sketch above is an example of this kind, where the fall has scarcely receded from
the lake shore. A slight indentation only is produced in the abruptly sloping bank of the
lake, and the same outline is preserved as if, on either side, it were stripped of its earthy
covering. The strata here are principally arenaceous, and offer little facility for rapid wear-
ing away; while at Lodi falls, a few miles farther north, where the principal part of the rock
excavated is shale, the fall is now about one mile from the lake. It is impossible to say,
with certainty, that these streams began their operations at the same time; though, if such
had been the case, they would never have receded at the same rate.
| |Wººl
iſºf º º : |º
§ {!
º º
|
º º º
ſº
|
|
º
|
|
|
º |Nº||
| |
| º
Emtramce of the Canaserowlie into the Caltaraugus creek.
In the more recently excavated channels we find the streams falling over the very edge of
the cliff, having produced no perceptible recession in the margin of the fall. The sketch
above is an example of this kind, where the Canaserowlie unites with the south branch of the
Cattaraugus creek. The channel of this latter stream is one of very modern excavation, as
might be shown from numerous facts, similar to those in relation to the Genesee about
Portage. The cliffs are almost vertical, to the height of one or two hundred feet, and the
gorge is narrow, presenting no deposits of drift. Its course is devious, however, and it some-
times enters an ancient valley, presenting a very different aspect from the recent one.
A series of observations, for one or two centuries, will enable us to speculate with some
degree of certainty regarding the probable rate of recession in waterfalls. But the observa-
tions require to be made at different points; upon streams of different magnitude; on falls of
different elevations, and upon those falling over different kinds of rocks. The rate of reces-
sion in one fall will be an unsafe guide for estimating that of all others. Accurate maps of the
WATERFALLS, 381
country, with monuments placed in situations where observations may be made, are the only
means by which this knowledge can be gained; and when the inhabitants feel sufficient inte-
rest in the operations of nature to establish and preserve such monuments, we shall be able
to arrive at important conclusions regarding the periods which have elapsed since these
streams began to wear their channels. Even with our present knowledge, these speculations
are not always unprofitable ; they lead us to take into consideration numerous influences
which ordinarily escape observation, and we often find that hasty conclusions are essentially
modified, or often changed, by the consideration of new facts. - -
The different rates of recession in waterfalls is shown when the successive rocks are of
different degrees of hardness, producing a series of falls. This happens where the highest
are more destructible than the lower, and by this means the upper fall outruns the others.
The Genesee river at Rochester presents an example of this kind, where the Medina sand-
stone, the rocks of the Clinton group, and the Niagara group, have each produced a distinct
fall. This, at one period, was doubtless a single cascade; but the upper shale wearing
away faster than the rocks below, allowed the fall to travel rapidly southward till it came
to the limestone surmounting the shale, where its progress was somewhat arrested. At the
present time it seems probable that the lower fall is receding faster than the upper, which
is thus protected. - - 3. - -
The following diagram illustrates the position of these falls, and the rocks over which the
water passes: - - . . . . ~
184.
-,--> * * *.* ~ *---> - -
* > -->
«sº sº
- º --- ‘s `. g : * > .T. gº * *g - -— ..." ºr * - --> - b
* * * * * - * -------, * ** * Eºrº,
# •º -E-2 a...T- . * * - > - * w * = v -- zºº., *** * :: *, * * * *_- - * * *
====º :===== - = −…" . " º ... = -- ..." – º –—"... • * , o, * Gº- ºr-a-gº-ºº-ººrs-a-Ti.
3. - 2. - I
1, 2, 3, Upper, middle and lower falls.
a, b. Medina sandstone. g. Shale of Niagara group.
c, d, e, f. Shales and limestones of the Clinton group. b. Limestone of Niagara group.
The upper fall is now upon the northern edge of the limestone, which increases in thickness
for two miles south, being a medium of constantly augmenting resistance; while the Medina
sandstone and the limestone of the Clinton group, are no thicker and no more difficult to wear
away than they have been for centuries past. Thus it is plain, that under otherwise equal
circumstances, the lower falls will advance upon the upper, until the whole will become one.
It will not then, however, be of the height of all these ; for the long rapid between the upper
fall, and the present place of the lower one, will be nearly as much descent as the fall at
present.
382 GEOLOGY OF THE FOURTH DISTRICT.
These speculations are offered, not with a view to any practical bearing, but to correct an
erroneous impression which arises from the first view of these falls. Since there are now
three falls, and since we suppose there was a period when only one existed, it is natural to
infer that the same cause that first produced a separation would continue to operate to per-
petuate the same condition. This would doubtless be true so long as the nature of the strata
remained the same ; but it is equally evident that any change in these will change all the
other conditions. -
2-3 º-3
E---> tº:
Eäß
º:
# =
=#
|
º
| º
jº. § º º
§º sº
sº sº
º |
º º ; tº | | º
º | |
§§|| #####|||}|\\\\\\ \ §
| º! | |. | | |
§ § * | § . §:
º É º § . §
É jº * §§§ § º º
- º
º
*\l
:º-
º
f
Wºº º
sº º º
§ sº flºº
*.….
£2-º’Žºg £gº
A. § §§
\: §§ § * gºººººº.º -º-º:
Lower falls of the GeneSee at Rochester. From a sketch by Mrs. HALL.
The lower fall at Rochester has evidently receded but very slowly for a long period; the
broad expansion in the river below evidently indicates that the falling water and eddying cur-
rents have done their work upon the cliffs for many centuries. Still within a short period the
stream has excavated the rock deeper upon the west side, and during the dry season nearly
all the water flows in that direction. This will eventually wear a narrow channel like the
lower fall at Portage, leaving a platform the original bed of the stream on the east side.
This locality offers a good exhibition of the succession of the strata. The Medina sand-
stone rises to the top of the falls, and is succeeded by the Clinton group, and this again by
the shale of the Niagara group. The layer of limestone containing the Pentamerus oblongus
is here one of the most prominent and interesting portions of the mass, while in the succeed-
ing shales occur the fossils figured under the Niagara group; thus presenting a succession
of the strata, scarcely so well exposed in any part of the district. x
::：：：:：…
ſae
:- :
Endicott Lith. N.York.
ĐÌ TRĪS ĢITĒ （TĀ VĪTĒVÝ (OTÈ TETT ANGĻĶĪRA ĪŅĀVĪLĪ, S,
------ ----
And the si IrroIIn dingCountry .
NIAGARA FAI, LS, 383
CHAPTER XX.
Niagara Falls, its past, present and prospective condition.
Among the phenomena of waterfalls and river gorges, the Cataract of Niagara is justly
regarded as holding the first rank, and as standing an index in the path of time, by which the
influence of numberless ages upon the surface of our planet may be recorded. Its present,
its former and its prospective conditions have engaged the investigation and speculation of
many philosophers. The possible consequences of its entire reduction, and the drainage of
the upper lakes, have excited the wonder and the apprehensions of many. The estimated
time of its recession has sprinkled grey hairs among the fresh locks of the young and blooming
earth, and alarmed those who would consider her still youthful in years. {
But amid all these speculations, Niagara still remains; the thunder of its cataract still
reverberates through its deep chasms, and its ocean of waters still rolls on as, unknown to
the white man, it rolled a thousand years ago. When we come to the investigation of facts,
we find that, except to travellers and the aborigines, Niagara was unknown until within the
last fifty years; and that even during this time no accurate observations have been made, no
monument erected to determine whether the falls are retrograding or not. The testimony of
living witnesses and historical evidence unite in confirming the opinion that the water is wearing
away the rock, and that the outline of the falls has changed. From these general observations,
it has been estimated that they have receded at the rate of about forty feet in fifty years.
Without pretending to question the accuracy of this or any other estimate of the kind, or to
establish any rate of retrogression in the falls, we may examine its present, and from nume-
rous facts infer its past condition; and from these we are entitled to draw an inference for
the future, though without specifying time.
Both in relation to the former condition and to the future recession of the falls, we may
regard the problem as undecided with respect to time. So many disturbing causes are con-
stantly presenting themselves, that, although the great principles may be regarded as esta-
blished, still it is impossible to calculate accurately the effect of these minor influences. The
recession of every mile changes the whole aspect: new elements are brought into operation;
the nature of the strata varies; the relative height of certain portions, and the elevation of the
whole cascade is altered; and we have had time to observe only one of the phases, and to
reason from that to the future, before the condition is changed, and we must take into the
account new influences, which the previous changes have called into operation.
384 GEOLOGY OF THE FOURTH DISTRICT.
The great difference in elevation between Lake Ontario and Lake Erie, and the occurrence
of the Cataract of Niagara, form one of the most striking features in the topography of Wes-
tern New-York. The difference in elevation of the upper great lakes is comparatively small;
they being nearly in the range of the strike of the strata, while the passage from Lake Erie to
Lake Ontario is directly across the line of dip.” Lake Erie is three hundred and thirty-four
feet above Lake Ontario, and the greater part of the descent from one to the other is overcome
by the rapids and falls of the Niagara river in the space of one mile.
The series of limestones forming the Helderberg mountains in the eastern part of New-
York, extend westward throughout the whole length of the State, gradually diminishing from
the thinning out of some of the members; and crossing the Niagara at the outlet of Lake
Erie, they extend far westward into Canada, and form, for many miles, the southern shore of
Lake Huron, and the eastern shore of Lake Michigan. This limestone dips to the south,
passing beneath the water, and forming to some extent the bed of Lake Erie. It forms the
second great terrace south of Lake Ontario, over the outcropping edge of which, on the north,
we descend to a low, level country, underlaid by the shales and marls of the Onondaga salt
group, which extends for fifteen or eighteen miles. Beyond this point there is a gradual and
almost imperceptible ascent for seven or eight miles, when we come to the edge of the first
great terrace overlooking the present valley of Lake Ontario. From this we plunge down for
two hundred and fifty feet, over the outcropping edges of various strata, which here terminate
abruptly, to the low table land bordering the lake. From the base of this escarpment, the
plateau, on which Lewiston and Queenston stand, slopes almost imperceptibly to the level of
the lake, which is seven miles distant, and one hundred and twenty feet lower.
A great portion of the country for twenty miles north of the southern terrace is so low and
level, that a rise in the river for thirty feet would inundate an extent of many miles on both
sides. The ascent from this low country toward the north is very gradual; but when we
arrive at the edge of the great terrace above Lewiston, the elevation is thirty-eight feet above
Lake Erie. The accompanying section from Lake Erie to Ontario, presents an outline of
this portion of the country. - -
This great terrace and escarpment, through which the Niagara makes its way into the valley
of Lake Ontario, is known in New-York as the Mountain Ridge, and in Canada as Queenston
Heights. It continues to the westward of Niagara river, curving around the head of Lake
Ontario, and thence trending westerly, some of its members extend beyond the Mississippi
river. To the eastward, it is distinctly traceable as far as the Genesee river; beyond which,
it merges in the general level, and the rocks forming it disappear almost entirely, from thinning
out, before reaching the Hudson river. The abrupt termination of these various strata upon
the face of the escarpment, prove conclusively the extent and effect of denuding agency upon
* The geological positions of Lake Superior and Lake Ontario, the highest and the lowest of this chain of lakes, correspond
very nearly with each other.
+ By means of the dam at Black-Rock, the water is taken from Lake Erie into the Erie canal, and carried through the Tona.
wanda creek, descending the terrace at Lockport by a cutting of less than thirty feet.
NIAGARA FALLS. 385
this part of the surface. The basin of Ontario, on the north of this terrace, has evidently been
excavated from the sedimentary strata; the limit of the force, and the extent of the lake basin,
being the line of this escarpment. -
It is quite unnecessary, in the present instance, to controvert the opinion which has been
advanced, of a dislocation of the strata, by which those forming the terrace have been elevated
to their present position. They are continuously exposed both on the north and south of the
escarpment, and it is very plain that no such change has taken place. The accompanying
section, and also the section, Plate IV., illustrate the order of succession among the strata.
Here, instead of any evidence of disturbance in the strata, we find the most unequivocal
proofs of denuding action, which has entirely removed the materials once forming the continua-
tion of these strata on the north. It will be seen that the strata, consisting of alternating hard
and soft beds, offer great facilities for the operation of any excavating force. The action of
water would thus undermine the harder beds, leaving them to fall by their own weight, while
the softer materials were removed. The manner in which this denudation was effected, and
the period of its occurrence, have already been noticed; and by the same means we are able
to account for this and other extensive lines of escarpment, where the succession of strata
presents a very different structure and ability to endure abrasion. In the same way we are to
account for the broad valleys in other situations, and the numerous gorges in the edge of this
escarpment. These are of little extent, scarcely reaching beyond a quarter of a mile, and
usually less; they present broad expanded openings on the north, and are very similar to the
indentations upon lines of Seacoast. *.
[GEOL, 4th Dist. 49
i
i
-
ſ
º
Ł, OMTAR10
Section of the strata along the Niagara river, from Lake Ontario to Lake Erie.
EXPLANATION OF THE SECTION.
1. Red shaly sandstone and marl, seen in the bank of the river at Lewiston, and
extending to Lake Ontario.
2. Grey quartzose sandstone.
3, Red shaly sandstone like No. 1, with thin courses of sandstone near the top.
4. Grey and mottled sandstone, constituting, with those below, the Medina
sandstone. +
5. A thin mass of green shale. -
6. Compact grey limestone, which, with No. 5, constitutes the Clinton group
at this place.
7. Soft argillo-calcareous shale. Niagara shale.
8. Limestone—compact and geodiferous. Niagara limestone.
8’. The upper thin-bedded portions of the Niagara limestone.
9. Onondaga salt group, including the hydraulic limestone, or beds of passage
to the next rock. -
10. Onondaga and Corniferous limestones, being all the limestones of the Hel-
derberg division which continue so far westward.
186.
•
f, g. The rapids, fifty-two feet, over the upper thin-bedded portion of the Nia-
Ž
a, a. A fluviatile deposit in the depression south of the Rapids, probably similar
to the fluviatile deposit of Goat island.
b, c, d, f, g, h. The dotted line represents the present surface of the river from
Lewiston to Lake Erie.
d, f. The perpendicular fall, over the Niagara limestone and shale.
gara limestone.
c. The whirlpool.
k, i, n. The position of the falls and rapids after a recession of one mile.
p, o, m. The position of the falls and rapids after a recession of two miles.
NIAGARA FALLS. 387
The strata 1, 2, 3, 4, 5, 6, 7 and 8, forming the escarpment at Lewiston as represented in
the section, are those through which the gorge of the Niagara is excavated; all that portion
above the dotted line b, c, d, as well as the depth of the river, being removed for a length of
seven miles and a width of twelve hundred to two thousand feet. These rocks dip gradually
to the south, and all below Nos. 6, 7 and 8 disappear beneath the level of the river before
reaching the falls.
The limestone which forms the summit of the terrace at Lewiston, and which at its margin
is not more than twenty feet thick, gradually increases from the addition of higher layers, till
at the Falls it has acquired a thickness of one hundred and sixty-four feet.* This limestone,
about one mile south of the Falls, disappears beneath the surface, and is succeeded by a soft
marl of a bluish or greenish-grey color. This formation, which is the Onondaga salt group,
occupies all the level country from two miles south of the Falls, to Black-Rock, a distance
of fifteen miles by the course of the river. To this succeeds the limestone terrace before
described, on the north of Lake Erie. -
The Onondaga salt group occupying this great breadth of country, and forming an important
item in any calculation regarding the future recession of the falls, had never been noticed by
any one till the publication of the Annual Reports of 1838. In all previous accounts the
distance from the Falls to Lake Erie was regarded as underlaid by limestone, and the lime-
stone of Black-Rock was represented as resting upon the Niagara limestone.
The Niagara river, from Lake Erie to its emergence into the low country at Lewiston,
has excavated a channel through the rocks represented in the section. The current, for
the first two miles after leaving the lake, is very rapid; after which it flows on more gently,
the channel gradually widening as far as Grand island, where it divides, the greater quan-
tity of water flowing on the west side of this island. Farther down, the river expands to a
width of two or three miles, and presents all the appearance of a quiet lake, with small, low
islands. The descent from Black-Rock to the head of the rapids is only fifteen feet. Ap-
proaching these rapids the river narrows and the current becomes more violent, and, for about
one mile before reaching the grand cascade, rushes on, with inconceivable velocity, over a
declivity of fifty-two feet, to the edge of the chasm, where it is precipitated into a gulf one
hundred and sixty feet below.f - -
The gorge through which the Niagara river now flows presents almost perpendicular walls,
with a talus at the bottom, formed by the falling of some of the higher strata. The outlet of
this chasm is scarcely wider than elsewhere along its course. In some places the channel is
less than two hundred yards across, and again is expanded to twice that width. The breadth
* Eighty feet only are visible at the Falls; its whole thickness was ascertained by levelling to Porter's quarry, a mile east of
the river.
# The birdseye view, facing page 383, conveys a very good impression of the face of the country, and the course of the river from
Lake Erie to Lewiston. A representation of the course of the river by this method was given by Mr. Robert Bakewell, jr., and
published in Loudon's Magazine of Natural History for March, 1830. This one was constructed without having Mr. Bakewell's
view before me, and the artist finished his work without seeing it. The idea of thus representing it was doubtless original with
Mr. Bakewell; but the same mode, to a certain extent, was adopted by Father Hennepin in his sketch which is given in this
chapter.
49*
388 GEOLOGY OF THE FOURTH DISTRICT.
of the chasm at the top is nearly twice as great as that of the stream below. The declivity
of the bed of the river, from the falls to Lewiston, is one hundred and four feet, or nearly
fifteen feet in the mile.”
At one place, about a mile below the falls, and where the channel is narrowest, the stream
glides with comparative stillness; while below this, where the channel is broader, it is driven
along with great velocity. Again, below the whirlpool the surface of the river is more
smooth, and the current more gentle, though the channel is narrower than above. These
appearances, which have seemed inexplicable upon the common theory, and which have been
used as arguments against the recession of the falls, have their cause in the geological struc-
ture of the place. Below the whirlpool there are no hard rocks in the bed of the river; con-
sequently the channel is deeper, and the water is more quiet than where such rocks exist.
At the whirlpool, and above that place, the hard sandstone No. 2 is at and near the level of
the river, and consequently the channel is not worn so deep. Again, after this hard mass has
dipped beneath the surface, the bed of the river is excavated in softer rocks; hence the nar-
row channel and smooth water a mile below the falls. Near the falls, the higher beds of
sandstone, and the limestone of the Clinton group, approach the level of the river, and thus
cause a wider, shallow channel, and more tumultuous water. Such I conceive to be the
explanation of the variable width of the chasm, and the greater or less violence of the water.
In the course of this gorge, there is a single exception to the parallel sides and nearly
vertical cliffs; this is upon the west bank of the river, at the whirlpool, as can be seen by
referring to the plate. Standing upon the east bank of the river, it appears like a depression
worn by the eddying current, which is partially obstructed in its course by the sandstone No.
2. Not having made particular examinations upon the Canada side of the river, I had over-
looked the true cause of this indentation, till during the summer of 1841, while in company
with Mr. Lyell, we examined this place, and found it to be an ancient gorge filled with drift,
except a narrow ravine through which a small stream flows into the river. In the channel of
this stream, near the river, there are one or two places where the rocks are exposed, proving
this gorge to be less deeply excavated than that in which the Niagara now flows. The ravine
may be traced for nearly two miles in a northwest direction, where it comes out to the gene-
ral level of the surrounding country. From the point of its termination, and following the
same direction for about one mile, we again commence descending through another deep gorge,
which terminates upon the plateau at the base of the escarpment at St. Davids, four miles
west of Queenston. It will be perceived by referring to the map, that the course of the river
before coming to the whirlpool, if continued, would lead in the direction of St. Davids.
From this fact it has been inferred that there is a continuous ancient gorge filled with drift,
from the whirlpool to this place. This inferencesseems substantiated by facts; for upon the
* A considerable declivity is required in the bed of such a stream, in order to give it power to remove obstacles which are con-
stantly impeding its course. In any stream excavating its own channel, the declivity of its bed will be, in some degree, pro-
portioned to the weight of the fallen masses which it has to remove; and if its channel be in soft shale, the descent will be very
gradual, while the intercalation of harder strata increases the descent according to their proportion.
NIAGARA FALLS. 389
elevated ground just before commencing the descent to St. Davids, upon the estate of the
late Governor Maitland, a well was dug to the depth of 150 or 160 feet, and the whole distance
in gravel and sand. This proves at least that the limestone has been deeply excavated, and
leaves no doubt in my mind of the continuity of this ancient gorge. This remarkable fact
has been cited as an objection to the opinion that the Niagara formed its own channel; but
still I hope to be able to show that its existence is equally an objection to the opinion that the
gorge of the Niagara was produced by the action of the sea. --
This ancient ravine appears to be filled with drift, of the period of the oldest drift of the
district; consequently we infer that it was one of the earliest effects produced by that denuding
agency which excavated all the great valleys of Western New-York. If this be true, it be-
came filled with drift before we have any evidence of any part of this region being above the
ocean, or of the Niagara river having an existence; therefore we have no ground for supposing
that it was ever the channel of this or any other river. If, on the other hand, we assume that
the present gorge of the Niagara was excavated by the ocean, and that the river has but cleared
out the drift, then we are bound to show that it resembles other gorges, which there is every
reason to believe that the ocean did excavate. The opening of the gorge at St. Davids, to-
wards Lake Ontario, presents a width of two miles where no rock is to be found in the line
of the escarpment; while that of the Niagara at Lewiston presents a width of fifteen hundred,
or perhaps two thousand feet. Allowing this ancient gorge to be continuous as far as the
whirlpool, wé find it to have diminished to a width less than the present river channel. In this
we see no analogy to the present channel of the Niagara, which, though variable in width, is
scarcely wider at its opening on the north than in some other parts of its course. If we
suppose that the undermining action of the ocean or an elevated lake aided in excavating this
channel, then also we must suppose that it would at the same time have removed the drift
from this ancient one; and if we suppose them both of the same age, or produced by the same
cause, then we should expect to find them similar in character, which is not true. The exis-
tence of this ancient ravine, so different in character from the present channel, indicates a
different origin; and as it corresponds with those gorges or indentations in coast lines, we
infer that it was due to similar causes; while that of Niagara, corresponding with all modern
river channels, or those which we know to have been formed by streams now flowing in them,
we infer that it, too, had a similar origin. - w --
It might appear more rational to conclude, that if the Niagara commenced excavating its
own channel, it would more readily find a way through the drift filling this ancient gorge, than
through a solid wall of rock; but this objection can be met by numerous examples, where old
channels have been closed by modern accumulations, and the stream has excavated a new one
through rocky strata. Such a case has already been illustrated in the passage of the Genesee
from Portage to Mount-Morris: in this example, the facts are incontrovertible; and whether
the Genesee ever occupied the ancient valley which is now filled with drift, does not affect
the conclusion; we see it leaving an ancient valley, through which it has flowed for many
miles, and entering a narrow gorge in the rocks of Portage, making a circuit of two or three
miles, when, by the ancient channel filled with sand and gravel, the same point would have
390 GEOLOGY OF THE FOURTH DISTRICT.
been gained in less than half the distance. Similar examples may be found in Seneca and
Cayuga lakes; the outlet of the former, instead of pursuing its course through an ancient
valley to Lake Ontario, turns to the eastward, and excavates a channel through the limestone
and gypsum beds between that lake and Cayuga.
Numerous similar examples might be cited, were it necessary, in order to account for the
fact that the Niagara did not take the course by the ancient ravine to St. Davids. In any
case it only requires that the superficial deposit should be higher than the rocky strata, and
that the water once be directed in that course, and it will wear itself a channel sooner than
remove the other deposit. --
In consideration of the argument that the channel of the Niagara has been worn by the
action of the sea, it may be necessary to offer some analogous examples. In all ravines, or
indentations, excavated in the face of sea cliffs, whether aided by a stream flowing in or not,
we find a broad or trumpet-mouthed opening toward the sea, and they recede abruptly to a
termination. They never present a long, narrow ravine of equal width; and where of a
length at all approaching that of Niagara, they have an opening many times broader than this
at Lewiston. Numerous examples of ravines formed in this manner might be mentioned, but
none of these resemble Niagara. In such instances they are broad enough to allow the
stream to flow in the bottom, leaving waterworn materials along the sides, monuments of the
abrading action of the waves. In the Niagara chasm there are no boulders, pebbles or gravel.
The river occupies the whole width at the bottom, except a talus on either side, formed by
angular fragments fallen from above.
The valley of the Genesee, from Rochester to Dansville, offers a good example of a chan-
nel excavated by the action of the sea during the emergence of land; but this valley is broad,
and partially filled with drift; the sides sloping gradually, and, for the most part, deeply
covered with transported materials. - - -
The small amount of wearing, or the recession of a fall, accomplished by a stream during
the period of our observation, might incline us to doubt the possibility of any body of water
having excavated its channel backwards for a length of seven miles, and to a depth of from
three to five hundred feet. But if the period of one life be sufficient to admit of observation
proving the smallest amount of recession, then it is only requisite that we should carry on the
process for an indefinite period, to accomplish the utmost that we require; or that we extend
backward our imagination regarding time, in order to demonstrate what is already accom-
plished. Now it is proved that within the recorded observations of persons residing in the
vicinity of Niagara, that the falls have receded within their recollection. Therefore, if we
are able to prove that this ravine could not have been excavated by the sea, during the
emergence of the land, we have only this mode of operation left to account for its formation.
It is barely possible that there may have been a fissure in the present course of this river,
which gave the first direction to the stream; but I have not been able to find any farther
evidence than what has already been given on this subject. I have remarked that the surface
of the limestone declines to the eastward, and I have been informed by Mr. Roy that it also
NIAGARA FALLs. 391
declines to the westward from Queenston. Such being the case, it is possible there may
have been a rent in this situation previous to the period when the river began to flow in that
direction. From all that appears along the present river course, there was probably an ancient
shallow valley extending in the direction of the present Niagara, which gave the first direction
to the waters. This will be made apparent by the following transverse section of the river
valley, which shows that the present square cut gorge is in the bottom of a previously formed
valley. Along the whole course of the river this gradual ascent from the edge of the gorge is
manifest, and, together with other circumstances, is evidently of the origin we infer.
From analogous facts, which have before been stated, we learn that it only requires an
elevation of drift or other superficial deposits greater than the rocky strata, in order to give
the water this direction, and cause it to excavate a new channel. In the present case it
only requires the depression before noticed, whether in the superficial deposit or in the
rock, to give the river that course; and, when it had once commenced flowing, no power
would divert it. Even if we suppose the channel to have been previously in any other
direction, if it became obstructed, the water would seek the lowest point along the terrace.
In the present instance this appears to have been in the direction of Lewiston, and here
the water commenced its work of excavation, cutting down the higher strata, and rapidly
undermining and removing those below. It is only necessary to refer to the accompanying
section, in order to discover what materials the river had to work upon at this period.
It is impossible that there could ever have been a perpendicular fall of the whole height of
the cliff at Lewiston, for the limestone at the top, being so much thinner than at the present
falls, would soon be broken down by the pressure of the immense body of water precipitated
over its edge upon the shale below. It may even be doubted whether the shale would be
excavated fast enough to form a perpendicular fall, and it is probable that the water would be
projected over a declivity of the upper shale (No. 7), to the limestone below, which, together
with the higher layers of the sandstone, would form the crest of a second fall. From this,
again, the water would be precipitated as far as the sandstone (No. 2), where a third fall
would be formed. Thus, instead of a single fall of three hundred and fifty feet, we should
392 GEOLOGY OF THE FOURTH DISTRICT.
have the whole height divided into three falls, at some distance from each other. In conse-
quence of the thinness of the upper limestone, that fall would recede faster than either of those
below it; and the middle faster than the lower one. Even under these circumstances, the
wearing action would go on much faster than at present. Finally, however, the recession
would become less and less rapid, from the thickening of the limestone above; and from this
cause, the two lower falls having only the same resistance to overcome as at first, would
gradually approach the upper, till the whole become one.”
At the same time there are other circumstances to be taken into consideration, and among
the most important of these are the dip of the strata and the ascent of the bed of the stream;
both together tending to bring the strata down to the level of the water as we progress
southward. This fact has also an important bearing upon the rate of recession; for while
a hard mass remains at a considerable height above water, with a soft one below, the exca-
vation of the softer one and undermining of the upper hard one, tends to the recession
much more rapidly than if the whole were of uniform character. Thus it must have been
that the fall over the sandstone (No. 2), receded much more rapidly while there was a
considerable thickness of shale below, than when it approached the level of the water. This
would happen after the falls had retreated about three miles, or nearly to the whirlpool. At
this point the recession would go on very slowly for a long period; for this hard mass, being
at the level of the water, would effectually suspend the undermining process. Even at the
present time this rock may be seen stretching into the river, from either side, beyond the
others, and at the point where it crosses, producing a descent of eight or ten feet within a few
rods.
After this long and almost stationary period at the whirlpool, the recession would again go
on more rapidly; soft materials being presented at the river level to be excavated by the force
of the falling water, which would thus undermine the harder mass above. -
When the cascade had receded to near its present position, another pause, similar to that at
the whirlpool, would occur, from the approach of the higher layers of sandstone (No. 4), and
the hard limestone (No. 6), to the surface of the water. There are various proofs of this
halting, both in the form of the chasm below the present fall, and from the fact that the higher
layers of sandstone still remain in place; for it is seen that having passed a few feet beneath
the water at the cascade, it supports the large fragments of the upper limestone which have
fallen down. . -
The conclusion then, seems inevitable, that the river has been the great agent in excavating
its own channel, from near the escarpment between Lewiston and Queenston, to the present
position of the cataract; that the recession has been aided by the character of the rocks, pre-
senting alternate hard and soft strata; and that the descent was overcome, not by one per-
pendicular fall, but by several. In support of this latter assertion, a single analogous case
will furnish stronger evidence than a long argument. The course of the Oak-orchard creek,
* See diagram on explanation of the falls of the Genesee, page 381.
NIAGARA FALLs. . 393
in Orleans county, is over the same strata, and exhibits the succession of falls and rapids,
precisely in the manner I have just enumerated. The quantity of water, however, in this
stream, is too small to produce any thing like a degree of recession to compare with the
Niagara river. . . = . . . s - - -
The following diagram will explain these remarks by showing the present position of the
falls and rapids along the stream; the numbering corresponds to that upon the Niagara sec-
tion, page 386: - . -
*-m-m-m-m-m-- . --------------- -
——----.... ---. --— —r-TTE:-trº-
Section along the oak orchard creek.
1. Lower part of Medina sandstone. 2. Quartzose sandstone. 3. Alternating, shaly and hard sandstone. 4. Greyband;
termination of the Medina sandstone. 5. Green shale of Clinton group. 6. Limestone of Clinton group.
7. Niagara shale. 8. Niagara limestone; falls at Shelby.
The same views have already been explained and illustrated, in relation to the falls on
Genesee river; but the quartzose sandstone (No. 2) of the Niagara section does not extend
so far eastward, and, therefore, it forms no item in the calculation at that place. The hard
limestone layer (No. 6), or one filling the place of that at Niagara, has retreated a quarter of a
mile farther up the river, where it forms a fall of twenty-five feet. This recession of the lime-
stone, beyond the sandstone, is owing to a mass of green shale below it, twenty-three feet
thick, while at Niagara the same shale is but four feet thick. From this place to the upper
fall, about a mile and a half distant, we have a rapid stream. This fall is one hundred and
ten feet high, and over precisely the same rocks as the Niagara fall at present, viz. Nos. 7
and 8 of section, the Niagara shale and limestone. The limestone at the top of the fall is
much thinner than that at Niagara, in consequence of the less recession into the mass, as well
as from being thinner as a whole. We have here a case precisely analogous to Niagara, as I
have supposed its former condition. - \ -
Had the quantity of water flowing down the Genesee been equal to the Niagara, the
upper fall would have been excavated farther backward, and the lower fall, in all probability,
entirely obliterated, presenting a rapid current from the upper fall to the present site of the
Rochester landing. There appears here positive proof that there never has been so large a
body of water passing down the Genesee as down the Niagara, and the concurring testimony
is to the effect that the wearing action has been far less. The recession of the lower falls at
Rochester would add little or nothing to the height of the upper; for the ascent of the river
bed, and the dip of the strata, would cause the disappearance of the whole beneath the water,
before reaching that point. - º
[GEoL. 4th DIST.] 50
394 GEOLOGY OF THE FOURTH DISTRICT.
In support of the hypothesis that falls do retrograde, we may adduce sufficient evidence.
Observations, during the last five years, upon the waterfalls of Western New-York, have
furnished positive evidence of their recession. Among these may be noticed the falls on
Jacock's run, near Geneseo, and Fall brook, a few miles farther south, both of which have
evidently receded, from the undermining of the platform over which the water is precipitated.
The amount during this time is very small, but quite sufficient to be appreciated. -
Lateral streams flowing into ravines or river courses, furnish the most palpable evidence of
the excavating power of water. The channel of Wolf creek, which comes into the Genesee
through a perpendicular wall of rock, is a good example of this kind, where the evidence is
conclusive that the excavating power is alone due to the stream. The junction of a small
stream with the Genesee, on the west side, below Rochester, furnishes another example of
this power. This stream has cut its channel through soft shale for fifty feet or more, a bed
of limestone eighteen feet thick, a bed of shale of equal thickness, and below this another bed
of limestone nearly equal to the upper one. Many more examples of a similar kind might be
named, on the Seneca and Cayuga lakes, and their valleys continued to the south.
All the historical evidence that we possess upon the subject proves the falls to have receded ;
and, although there have been no monuments established, yet the representations of early
travellers, when compared with the present condition of the falls, proves that a change has
taken place, though we cannot be certain of its precise amount. * *
The oldest authentic historical account of the falls which I have seen is that of Father
Louis Hennepin, who travelled in this country in 1678.* The accompanying view of the
falls is a facsimile of that published in his travels, and though rude and fanciful, it is, in many
points of view, highly interesting and important. > . -
It represents a projecting rock upon the west side of the river, which turned a part of the
water across the main fall, as seen in the sketch. This fact is of great interest as showing
one important change which has taken place within the historical era; for in regard to a
portion of the water being projected from west to east, forming a cross fall, there seems no
doubt, as it is particularly described. In chapter LXX, he says, “From the end, then, of this
island it is that these two great falls of water, as also the third, but now mentioned, throw
themselves, after a most surprising manner, down into a dreadful gulph six hundred foot and
more in depth. I have already said that the waters which discharge themselves at the cas-
cade to the east, fall with lesser force; whereas those to the west tumble all at once, making
two cascades; one moderate, the other violent and strong, which at last make a kind of
crotchet or square figure, falling from south to north and west to east.” The northwestern
* This work is entitled “A New Discovery of a Vast Country in America, extending above fourthousand miles, between New-
France and New-Mexico; with a description of the Great Lakes, Cataracts, Rivers, Plants and Animals; also, the Manners,
Customs and Languages of the several Native Indians; and the advantages of commerce with these different nations, &c.” Dedi-
cated to His Most Excellent Majesty, William III. King of Great Britain, &c. By F. Louis Hennepin. London, 1698. This
work was first published in Utrecht in 1697. . - . . . . .
My attention was called to this book and view of Niagara falls by Joseph W. INGRAHAM, of Boston, who has given much
attention to collecting the historical accounts of Niagara falls. - - --
XLIOAN VIII I Loompwa）
^{} 69 I“unda III： H.sino'ſ Jølſe）{Åų.
‘STITŪTĀ Vºtºſ@ſº II，
dº ºſº º dº ſºlſ|Iſ]] ©
ſae|-
ſae
|----
NIAGARA FALLS. 395
end of Goat island is also represented as extending perpendicularly to the water; and though
we can hardly credit this, we can conceive how such an error may have been committed;
when the spot was inaccessible.
In 1750, Kalm, a Danish naturalist, visited the falls, and his description and view is publish-
ed in the Gentleman's Magazine in 1751. His general description corresponds with that of
Father Hennepin, though there was at that time no third cascade. The period of his visit
was seventy-two years after that of F. Hennepin, and he distinctly alludes to the projecting
rock, which forced the water out of its direct course, causing it to fall across the great fall.
He speaks of this rock having fallen down a few years previous, and in his view of the falls
the spot is indicated. In this interval of seventy years we find that the recorded observations
of these two travellers prove precisely the same kind of change to have taken place, as we
suppose to have occurred previously, and which has subsequently altered the outline and
position of the falls. - -
We have not space here to introduce all the subsequent accounts of Niagara falls which
have been published, neither would they furnish us with arguments bearing upon their reces-
SIOIl. -- º
In 1824,” Prof. Eaton gave a section of the rocks from Lewiston to Lake Erie, which, with
the omission of the Onondaga salt group, corresponds with subsequent observations. This is
the first account of the falls which I have seen where the geological structure of the place is
given. - - - - --
In the 28th Vol. of the American Journal of Science and Arts, Prof. H. D. Rogers has
given a very full description of the falls, and the geology of the surrounding country, together
with his views regarding the formation of the chasm of the Niagara, and the future recession
of the cataract. - - t
Mr. Hayes, in his paper on the geology and topography of Western New-York, f has pre-
sented many interesting facts and speculations relating to the falls and the production of this
chasm, as well as the fluviatile deposit of Goat island and the eastern shore.
We have now to consider another class of phenomena, which aid us in our conclusions
regarding the recession of Niagara, proving at least that the water has extended much farther
in the direction of Lewiston before the present gorge was excavated. The nature of this
evidence I pointed out in my report on the Fourth Geological District of New-York, in 1838,
pages 271, 272, and 273. At that time, I was not aware that the same phenomena had before
been noticed, though I have since learned that the existence of freshwater deposits on Goat
island was known some years previous. Whether the important inference had been deduced
from this fact or not, I do not know. - -
Goat island stands upon the top of the precipice separating the two falls; it is formed by
the accumulation of gravel, sand, and clay, upon the surface of the limestone, and is evidently
* Geological and Agricultural Survey of the District adjoining the Erie Canal, Part I. page 149.
+ Am. Jour. Science and Arts, Vol. XXXV. No. 1. -
50*
396. GEOLOGY OF THE FOURTH DISTRICT.
a portion of a once much more extensive deposit. Upon the southern side of this island,
where there is an escarpment, the thickness of the superficial deposit is about twenty-five
feet. The upper half consists of coarse gravel and sand, with abundance of fresh water shells
of the genera Unio, Cyclas, Limnea, Planorbis, Valvata, and Melania; the same, both in
genera and species, as those now inhabiting the river and lakes. The occurrence of these
shells, in this situation, about forty feet higher than the top of the fall, proves the existence
of a river or lake at an elevation sufficient to allow of such a deposition, for this accumula-
tion of shells and gravel bears all the evidence of a fluviatile deposit. It is equally evident
that this deposit could not have been made while the falls were in their present position.
During a reëxamination of this place in 1841, in company with Mr. Lyell, we discovered
the Cyclas, Walvata, &c. in a terrace, upon the east side of the river, of the same elevation as
Goat island. It was at this place, and in the same deposit, that a Mastodon’s tooth was
found eleven feet below the surface. Farther northward, and more than half a mile north of
Goat island, in another excavation, we discovered similar shells. At the same time we noticed
the continuation of this terrace as far as the whirlpool. Since that time I have levelled the
whole distance from the falls to the whirlpool, and find the elevations at the two places to
correspond. Shells are even more abundant in this terrace at the whirlpool than at the falls."
Farther north than this point, I have made no examinations for freshwater shells.
Upon the west side of the river there is a similar terrace, which is mentioned by Mr.
Hayes as also containing freshwater shells,f in common with that on the east side. Now, in
order to find a barrier on the north sufficient to elevate the water so as to make this deposit, it
would require to extend it far towards Lewiston. Furthermore, it is evident that the deposits
forming these banks or terraces, on either side of the river, and that of Goat island, were not
made in this form, but are parts of a once much more extensive formation, which has been
removed by the waters of the river. During the time of its deposition the river must have
occupied this ancient valley, which extended toward Lewiston, finding a barrier much nearer
the edge of the terrace than the whirlpool. In the bed of this expanded river or lake, much
as it now is above the rapids, this deposit was made, probably covering the whole extent.
From the subsequent recession and drainage, the margins only have remained, together with
Goat island, indicating its former extent. The position of this fluviatile deposit, which is
subsequent to the ancient drift, may be illustrated in the following diagram: +.
* See accompanying map and elevations. Mr. Lyell informs me that in a second visit to the falls in the spring of 1842, he
found freshwater shells at the Whirlpool. - - - -
# Am. Journal of Science and Arts, Vol. XXXV. No. 1.
NIAGARA FALLS. 397
189,
. Limestone.
, Shale.
a. The terrace with shells on the eastern side. c. The terrace on the Canada side.
b. Goat island. d. The ancient drift.
From the present position of the remains of this deposit, there can be no doubt but it was
once continuous, the greater part of it having subsequently been removed. The mode of its
formation can be well illustrated by referring to fig. 186, a, a, which is intended to represent
what is now going on in the broad expansion of the river above the rapids. This fluviatile
deposit is made by materials brought down by the current, and doubtless mingled with a
large accumulation of shells of Unio, Melania, Anculotus, &c. as these shells are abundant
above the falls, and large numbers of the shells of Uniones are constantly brought down the
rapids during the summer season.
The single terrace containing shells is not the only one; on the eastern side, at lower eleva-
tions, there are in succession three others (as seen by the acompanying topographical map of
the falls), which seem to be remains of the deposit in the river bed, as it successively exca-
vated its barrier on the north, and receded towards its present position. For the greater part
of the distance from the falls to Black-Rock, on the eastern side there is a terrace or bank a
few feet higher than the river, which may have originally limited its waters when it stood at
the level indicated by the freshwater deposit of Goat island. Near Black-Rock, and border-
ing the valley of the Tonawanda, there is a terrace some twenty feet higher, which appears
to have been the boundary of the river or lake at a still earlier period; but with these we
have, at present, nothing to do. The existence of the fluviatile deposit of Goat island, and at
the same level on the eastern side of the river, requires for its elucidation the existence of
water standing at a level somewhat higher, in order to allow of the deposit being made in the
bed of the stream. To accomplish this, a barrier is required further north than the Whirlpool,
and about the height of the surface of limestone between this and Lewiston. The occurrence
of successive terraces below this one, proves that the drainage to the present point was not
effected suddenly.
There is another fact which should be noticed, as proving the existence of a current from
south to north, during the deposition of the materials forming Goat island. The pebbles, at
least large numbers of them, are of the limestone of Black-Rock, and the harder layers of the
Onondaga salt group, like the rock in place at the upper end of Grand island. The surface of
the rock, on which the deposit forming Goat island is made, is smoothed and scratched, as
398 GEOLOGY OF THE FOURTH DISTRICT.
are the surrounding surfaces, both in the rapids and on either bank of the river. The deposit
is of greatest thickness towards the fall, and thins entirely out at its southeastern extremity.
In some places the lowest part of this deposit is of clay, which has been subsequently covered
by gravel and sand, containing the freshwater shells. This proves the first condition to have
been that of a quiet lake, while subsequently a current, transporting pebbles and sand, passed
over the same bed, leaving the coarse deposit.
There is another indentation on the eastern bank of the Niagara, below the Whirlpool.
This has been cited as a case where the small stream coming in, is insufficient to account for
such an excavation. It occurs at the junction of Bloody run and the river, and bears the
strongest evidence of having been produced by the common agents, frost and water. The
wearing action of the stream alone is probably insufficient to produce this short ravine, which
extends a few rods back from the margin of the river bank; but when we take into considera-
tion the fact, that the water penetrates all the fissures of the rock, and then, during fall and
winter, expands by freezing, we shall find means of explaining the mode of operation. At the
falls, the recession is by the undermining and breaking down of the upper masses; the action
of frost is not to be taken into consideration, as the water, probably, never freezes in the fissures
behind the fall. Now I consider it as an established fact, that small streams, which freeze
during winter, will excavate their beds more rapidly in proportion than large bodies of water
which never freeze. It appears to me that the indentation at Bloody run is not greater than
might be expected to have taken place while the main channel receded to its present position.
Whatever facts and arguments may be advanced to prove the existence of phenomena indi-
cating the former action of the sea in excavating the Niagara channel, and whatever objections
may be advanced for or against other theories, I am fully convinced, from the facts presented,
that the existence of the falls and the Niagara river, in their present position, is of very recent
date geologically. -
We come now to consider the future recession of Niagara falls, and its consequences.
This is a subject on which many speculations have been hazarded, but no one appears to
have undertaken the calculation with a full knowledge of the geology of the district, or to have
taken into account the many disturbing influences. At the present time, the cliff over which
the water is precipitated, is nearly equally divided between thick-bedded limestone and soft
disintegrating shale. It is by the action of the spray from the falling water upon the shale,
undermining and leaving the limestone unsupported, which falls down by its own weight,
that the falls recede from their present position. Now if we believe the statements of those
who have resided at the falls, the recession has been about fifty yards within the last forty
years; but from all the data I have been able to obtain, this appears to be much too great an
estimate; indeed, it is extremely questionable if the fall has receded as many feet within that
time. The central portion of the Horseshoe fall recedes more rapidly than any other part,
for here the greatest force of the river is exerted. We know, likewise, from the testimony
* Am, Journal of Science, Wol. XXXV. No. 1.
NIAGARA FALLS. 399
of all residents at this place, that the American fall is becoming more curved in its outline,
whereas formerly it was nearly in a straight line. The successive descent of large masses
of limestone, and the still continued overhanging of the table rock, prove very conclusively
the unremitting action of water and air upon the shale below. " . - - .
In the absence of established landmarks, we are compelled to leave the rate of recession
unsettled for the present. The accompanying trigonometrical map of the falls will furnish
the means of doing this, by the monuments which have been established, and which may
be considered as permanent points of reference for the future. º
Leaving out of view the time or rate of recession, we have sufficient data to establish with
certainty the future changes which will supervene, allowing the recession to go on as it is now
doing. The lower half of the rock at the cascade, or about eighty feet, is of soft shale, the
limestone above being of equal thickness; higher still is about sixty feet of thin-bedded
limestone, forming the rapids. These different rocks are represented in the section as 7, 8
and 8', respectively. Now these beds dip to the south at the rate of about twenty-five feet
in the mile, and the declivity of the bed of the river is about fifteen feet in the mile from
the falls to Lewiston. It follows, therefore, that as the falls recede, there will be a less
amount of shale above water, owing to the dip; and to this must be added the amount of
declivity in the river bed, both together making forty feet. So that when the fall has receded
one mile, the surface of the water will stand at k, of section page 386, or a point in the shale
half way between the present surface of the water and the bottom of the limestone. Going
on at this rate for another mile would take away from the fall forty feet more of the shale, so
that the surface of the river would then stand at p, or the base of the limestone.
The cataract would then have a solid wall of limestone to wear down, the river beneath
protecting, in a great measure, the undermining action upon the shale. During this time, and
at the end of the first mile, the falls would have arrived at the present site of the commence-
ment of the rapids, and thus about sixty feet more of limestone would be added to the height;
unless from its thin-bedded character it continued to recede faster, and thus remain a rapid.
In this case, there would be a fall of one hundred and forty feet at the end of the first mile
(i, k); and one of one hundred feet (o, p) at the end of the second mile. -
At this period, then, we are to contemplate the cataract of Niagara as having receded two
miles, the shale having disappeared beneath the river, and the cascade presenting a solid wall
of limestone one hundred feet high, and a rapid of forty or fifty feet (o, m) beyond. The
recession will then go on very gradually; and so soon as masses from this cliff have fallen
down to fill up the river bed, as they inevitably will in a great measure, then the base will be
protected so effectually that little influence will be exerted by the force of the water. Even-
tually, however, the cliff will be broken down, and huge fragments piled up below, until the
cataract will be nearly lost amid them. This state of things will continue for a long time,
the height gradually diminishing, till the river has cut its way back for two miles further,
when there will be no thick-bedded limestone above water, and the higher beds will form a
rapid as before. - - -
400 GEOLOGY OF THE FOURTH DISTRICTs
This point of meeting between the surface of the river below the fall and the top of the
thick-bedded limestone, will be about one hundred feet lower than the top of the present
cascade; and as there will be forty feet of rapids in the thin-bedded limestone within a short
space, as there now is, it follows that there will be added to the descent of the river beyond
the rapids, one hundred feet more than at present, as the surface of the limestone has dipped
to that amount. The whole fall in the river at that time, from Lake Erie to the point of
junction between the limestone and water below the rapids (h, o], will be about one hundred
and sixty feet. The distance between this point and the outlet of Lake Erie is occupied by
nearly uniform soft layers; and after a partial wearing down of the limestone forming the
rapids, the descent will be equally distributed over the whole extent of sixteen miles, giving
a uniform declivity of about ten feet in the mile, or one-third less than the present declivity in
the bed of the river from the Falls to Lewiston. From the nature of the bed of the river for
sixteen miles below Lake Erie, it may be doubted whether this rapid descent along the whole
distance would be continued; for the stream, having no heavy blocks of rock to remove, would
keep its channel clear with a far less declivity; and should this prove the case here, we
might still have a fall of a few feet, at the outlet of Lake Erie, over the limestone succeeding
the salt group. -
Whether such a fall would occur, depends on the solution of the problem regarding the
required declivity in the bed of the river below Lake Erie. Whichever way it may occur, it
will make no material difference in the great result, which will be either a continuous rapid
stream from Lake Erie to Lewiston, or a rapid stream with a low fall at the outlet of Erie.
If present causes continue to operate as now, such will be the consummation of the grand
cataract of Niagara. -
It is unnecessary here to follow on this recession gradually from the outlet of Lake Erie to
the final drainage of a portion of its waters. The views which have been entertained of
the sudden drainage of this or any of the upper lakes, and a deluging of the country on the
north and east are no longer considered as tenable by any one; and even if Lake Erie could
be drained suddenly, it would cause no deluge of any importance. If the whole lake were
at once placed upon Lake Ontario, it would only elevate its surface by about one hundred
and fifty feet, so that its extent would not exceed the limits of the ancient lake ridge, and the
outlet would still be the valley of the St. Lawrence.
Thus far the country supplying water to the upper lakes has been but little changed by the
hand of cultivation; the primeval forests still clothe the surface, and evaporation, to a great
extent, is prevented. This cannot always remain so; the advancing settlements will yet
penetrate even to the wilderness bordering Lake Superior, and the opening of the surface to
the influence of the sun's rays will greatly diminish the supply of water flowing into its
tributaries. These causes will sensibly diminish the quantity passing down the natural out.
let; and the mighty Niagara is destined to be, at certain seasons, but a diminutive represen-
tative of its former grandeur.
NIAGARA FALLS. 401
But this event, though a certain result of existing causes, must still be inconceivably dis-
tant; and Niagara, for thousands of years, will continue to be the Thunder of Waters, whose
magnificence no pen can describe, no pencil can express; which to be appreciated must be
seen in its vast tumultuous waves, as they sweep down the rapids and are hurled into the
immense chasm below, and heard in its voice of thunder, which drowns all other voices, and
reverberates in one perpetual roar of sound and echo,
NoTE.—The quantity of water flowing down the Niagara river has been variously estimated by different observers.
Mr. Dwight estimates the amount at.................. 361,392,742 cubic feet per minute.
Mr. Darby, . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 27,878,400 & & § {
Mr. Pickens, . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 3,087,533 { { { {
Mr. Barrett, . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 19,500,000 {{ § {
The last estimate is from three different observations made at Black Rock during the high water of 1838 and 1839.
The extremes of all the observations did not vary more than 20,000 feet per minute.
Mr. Barrett informs me that the quantity of water taken out by the different canals is as follows:
Erie canal, 30,000 cubic feet per minute.
Welland canal,” 7000 cubic feet per minute.
Illinois canal, from 5000 to 10,000 cubic feet per minute.
In addition to this estimate, there is a considerable waste of water along these canals, which is not taken into the account.
All these amounts are small when compared with the great body of water flowing into this channel, and we can scarcely
suppose that this abstraction will produce any appreciable difference in the rate of recession; but there are other causes
which will certainly produce an important diminution. -
* This amount will be greatly increased by the enlargement of this canal.
[GEol. 4th DIST.] 51 **
402 GEOLOGY OF THE FOURTH DISTRICT.
Trigonometrical Survey and Map of Niagara Falls.
The accompanying map has been constructed from a very careful survey by Mr. Blackwell,"
giving the present position and outline of both falls, and the river banks upon either side.
Upon application to His Excellency Sir Charles Bagot, late Governor-General of Canada, I
was authorized to establish monuments upon the Canada shore, and was also kindly offered
every other aid to promote the objects of the survey. These monuments, together with those in
New-York, will enable future observers to ascertain the amount of recession during any given
period. In places where the rock is exposed, copper bolts have been fixed, and in other places
hewn stone monuments. The starting point for all these observations is a copper bolt fixed in
the rock on the north side, near the edge of the American fall; the trigonometrical point No.
1, is thirty-nine feet four inches north, 80° east from this. These points are connected with
T. P. No. 2, so that in the event of those nearest the cliff being undermined, the latter can be
resorted to. The accompanying table of observations will serve to reconstruct the map so .
long as any of the points remain. -
The following are some of the elevations noted at the time of this survey:
Height of American falls, October 4th, 1842, . . . . . . . . . . . . . . . . . . . . . . . . . . . . 167.70 feet,f
Height of Canada or Horseshoe fall, . . . . . . ............................ 158.50 “
First terrace, height above top of fall at the point before mentioned,.......... 14.75 “
(The surface of this terrace is uneven, with scattered fragments of limestone,
appearing like the bed of a river.)
Second terrace, . . . . . . . . © e º & e º se & e º ſº e • - - - - - - - - - - - - - - . . . . . . . . . . . . . . . . . 24.09 “
Third terrace, . . . . . . . . . . . . . . . . . . . - - - - - - - - - - - - - - - - - - - . . . . . . . . . . . . . 32.42 “
Fourth terrace, (the one containing shells), . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 39.79 “
This terrace slopes upward to the railroad, a height of . . . . . . . . . . . . . . . . . . . 46.20 tº
General level of Goat island, corresponding to that of the fourth terrace, ..... 39.86 &
Top of highest terrace at whirlpool, . . . . . . . . . . . . . . . . . . . ................ 70.00 tº
Base of this terrace, or level of the bank at the same place, ................ 46.98 tº
Shells were found in a fine clayey loam at the whirlpool, at an elevation of ... 33.03 &
More abundant at. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 35.00 {{
And continuing upward to. . . . . . . . . . . . . . . . . . . . . . . . . . . ................ 46.00 tº
*This survey was made in the fall of 1842, though the observations had been principally made by Mr. Blackwell in 1841; but
as no permanent monuments had been established, it was thought better to review the whole. Through the kindness of Mr. Fay,
the resident engineer at Lockport, Mr. Gibson and Mr. T. Evershed were directed to accompany me, and, together with Mr.
Blackwell, to make the requisite observations and run the levels, all of which are shown upon the map.
# This elevation is from the level of the water below the falls to the copper bolt near T. P. No. 1
• The elevation varies from
four to twenty feet with the elevation of the water in the river below the falls.
‘../222767/7 27/123
Ža.41%2227g y 7
‘2/22/(Z S32/222// S. Aſ
zºa 2 2*º 22° 22′. º 22*. º, ſº º *g
JO G, TITV4 o'll J0 A3/\}|ſ|G, TW/ºilſ. Hiſlº. [A][]|N|[ſ] [I]]|| ||
****
§ Williw)
º wº
W}\{{D\/|N
\ N/\\
Wºº
' ' |\ \\
|
|
|
|\\
| &\\\\ \
\
} \ .*.*
º
* i. == is.
* \\ § º %||||Wiśiñº
\ § à. }\ \\\\
s s|
W. | | \ §
i
\
º:
£2.
Axe QI É*
º \N
/|| |WN
|\\\\\\\\
|\ \\\\
sº
\
\
&,
-: 2
|
|
/
|
|
|
==F.—
se-I. Z
§
Y "ºffº = Y \}
*z
--> s
/
/
*
WW
wº
wº º
ſ | t \º - *
\
N
§º
%
% º|
wº
tº
!II111]]
º
sº
º
§§ r
§ #
§§º
- §).2
§§
. be: &
s
with
|
\
§§
$º
ºulº.
º N/
º
gºš
**
g - º - - Y!
§/|N|
SW N Z |
º º |
Nº. // | N
|
\
\
\
\
^
N
* // ;
A → 2
/ 2'
A .
F-4 -2 A
/77–
/ .* /
|
..-
-
-2
§
tº #
{ *
|
|
,!|
|\
}}
V (I v N v o
º
|| N
NN/
* N !///||
º \}
... * * º/N \%|N
nWº. SS
QS
• { -
wº º
* wºulº *W | |
wº jº ſº sºNºſ. - W
gº \ *ś #s: :º
: É 3: §: =s
y A * ,
- *N
\
g &
ºś
N
§
§s
§
N
N
º W
\\
.S.
. º -
º 47% |
N
'N
N
WN S
§
\
|
|
N g
| \
º
º º,
&
3.
sº
Q
*-
&
& ovº
*
2.
*
s
à
3..
<o
|
-º§
- *.3.º-
'.32
&
º
ºº.
º
|
º
WN/ >
§º
Q §§§ º Y is
§§ Ç §§º -
§§C #&
gº
f
§§ ść. Ç
lſº
º
3.
&
sº
* º ſ f
& Lé - %
ſº ãº
| :Sºſiiº
ſ !" § ºf E
&
t
§
§
> s\\
\ 2- §
sº>
|
<&
&
ss-
S - º # \ § & º § *.
s º Nº
NS §seº %
SS-Sº sé% f
SN ...”
ſ
§
&
^. - S--> - --
Šº ... --- **
\ ^: * * * -- ------ --
\ X-J :2:…”
-** ~II 2. “A.”
§
§ 2. wº Nº *---
*Nºlº # §§§ *
*º- §ll! $º Y - - f S$ *
*šº º * \\\ § --~ ~~~ º º $
% º Šs- * \S Š §: - ) ---. (' i sº §§§ . . .
2% * - * º # %===S \\\\\\\\ ; sº . . . ."
& - X) & % NSºsyº. \\ § s' " -
~ O *%-ºšNº sº
ſ \, % %. \ ſº ź # &N is §§ | : \ | ſº y § § w
- - - £º (((((ºft §º wº * § \\\\\\\\\\% #. Sº ,
sv \s */ \ * is NWA Wº º sº ...,
:= } </j/? * º- - | | | | | | | - -ºš -
- º lſº º)" \\# -
*...arºS - 2%ij}} \\\\º
V § º %). \\\\\º
QNº-º-º/\º
:::::13.2%), : \\\\\\\\\ §.
*/0))) "||}) \ | § {
$WN
\\ &
§ §N Šsº:
ºšē
NIAGARA FALLS, 403
It will be seen that the elevation of the point where these shells occur at the whirlpool cor-
responds with Goat Island and the fourth terrace on the east bank of the river. This can
leave no doubt that these points are portions of a once continuous deposit, and it is not im-
probable that it may be traced still farther to the north. It will be recollected that the tooth
of a mastodon, and shells of Cyclas and Valvata, were dug from the fourth terrace, eleven feet
below the surface, or about four feet lower than those seen at the whirlpool, though these may
have extended as low. In the terrace at the falls, these shells have not been found at an
elevation so great by about six feet as at the whirlpool. -
51*
404
GEOLOGY OF THE FOURTH DISTRICT.
gº º
& O
e Q
º “e
• *
tº º
tº º
gº º
tº e
tº º
© Q
tº b
- ©
e e
gº º
& ©
e -
tº 0
tº º
- tº
tº @
Q &
- e.
tº tº
© &
© tº
o º
gº º
tº º
tº Q
tº º
© tº
- o
tº tº
© º
|Trigonometri-
cal Points.
==s**-*-*
From No. 1
TABLE OF OBSERVATIONS
course. . [...] Tº course. ...Tº course. ...
N660 35/E60ft to No. 1 ||From No. 5 || S 49930/W to No. 31 ||From No. 7 | S 61953/E | to No. 2
N 86020/ W | . . 2 ... . . S 37 50 W . . 32 ... . . S 56 30 E | . . 3
S 70 0 W . 3 || .. . S 49 0 W . 33 || . . . S 52 45 E. 4
S 33 5 W . . 16 || . . . . |S 65 0 W . . 34 || . . . . S 49 30 E | . . 5
S 19 0 W | . . 19 . S 72 0 W . . .35 - e. & e - tº G . . 6
S 11 55 W . . 20 gº tº . S 88 50 W . . 36 tº º . S 48 15 E | . . 7
S. 8 0 W | . . 21 . . . . S 80 45 W . . 37 || . . . . S 46 45 E | . . 8
S 1 1 0 E . . 22 ... . . S 70 40 W | . . 38 ... . . S 44 0 E | . . 9
S 15 50 E . 23 . . . . S 63 30 W . 39 - gº S 43 15 E. ... 10
S 16 50 E º • 24 º ºg & e S 51 15 W º 40 & O. º e S 39 15 E. e 11
IN 25 0 W . 48 . . . . S 37 30 W . 41 - e. S 38 30 E | . . 12
N 46 10 W . 49 . . . . S 37 40 W . 42 © º . S 37 5 E | . . 13
N 67 30 W . . 50 ... . . S 27 50 W . . 43 . . . . . . . . . . 14
N 73 30 W . . 51 ... . . S 17 40 W . . 44 . . . . S 33 5 E | . . 15
S 85 0 W . 52 . . . . S 8 50 W | . . 45 . . . . S 19 20 E | . . 47
N 31 45 W . . 56 || . . . . . S. 70-15 W | . . 46 || ... No. 8 N 74 27 E | . . 4
S 74 45 W . . 16 ... . . N 73 30 W | . . 53 . . . . N 78 57 E | . . 5
S 41 45 W . . 19 tº tº . N 54 30 W . . 54 tº . . N 80 0 E | . . . 6
S 38 0 W . . 20 . . . . N 59 10 W . . 55 © Co . N 81 27 E | . . 7
S 40 45 W . . 21 ... No. 6 | N 68 15 W . . 28 || . . . N 82 40 E | . . 8
S 14 05 W . . 22 . . . . N 76 O W | . . 29 tº gº N 83 27 E | . . 9
S 8 40 W . . 23 . . . . N 83 30 W | . . 30 tº gº . N 84 40 E . 10
S 5 20 W . . 24 . . . . S 86 0 W . . 31 © Cº. . N 87 0 E . 11
N 31 30 W . . 48 ... . . S 65 0 W | . . 32 tº o . N 88 7 E 12
N 55 30 W . 49 . . . . S 71 15 W . . 33 tº Q . N 88 50 E . 13
N 78 30 W . 50 ... . . S 85 0 W | . . 34 tº º . S 89 45 E. . 14
N 82 0 W . . 51 . . . . N 88 30 W | . . 35 © tº S 77 45 E . 15
S 77 45 W . 52 . . . . . N 75 20 W . . 36. tº tº S 69 15 E . 47.
N 424 E 100 ft . 17 . . . . . N 84 0 W | . . 37 tº º S 34 55 E . 25
N 48 30 E 46ft , 18 . . . . S 83 40 W | . . 38 tº º e S 30 15 E . 26
S 70 45 W. . 53 . . . . S 77 30 W | . . 39 . . . . S. 25 30 E . 27
S 85 45 W . 54 . . . . S 63 10 W | . . 40 || ... No. 9 || S 88 25 E . 25
S 88 50 W . 55 . . . . S 47 0 W . . 41 . . . . S 85 25 E . 26
N 6 30 W . 56 . . . . S 45 50 W | . . 42 tº º S 82 5 E . 27
S 68 45 W . 28 . . . . . S 36 15 W | . . 43 tº º S 68 10 E . 29
S 61 15 W. . 29 tº ſº º º S 29 15 W. . . 44 © tº S 62 4U E . 30
S 55 30 W . 30 tº e . S 16 45 W | . . 45 º S 54 50 E . 31
gº tº . N 56 30 W \ . . 46 || .. S 40 10 E 32
Stone Monuments set at Trigonometrical Points No. 1.2, 5, 6 & 8, and one set N. 68° 10' W. 2.00 Chs, from ||
T. P. No. 6.—CoPPER BOLTs set at Trigonometrical Points No. 7. & 9, one set S. 67° 30' W. 72, feet from T. P. ||
No. 9, and one set S. 80°30' W. 393 feet from T. P. No. 1.
LAKES. 405
§ SU
§§§ E=
§§ WSE====
§§ Sº š==#=#
§§ ===== >†:
sºrº º
- ºš § à 3%3 % º
ść 㺠% * £%
Conesus Lake. From a sketch by Mrs. HALL.
CHAPTER XXI.
LAKES.
Lakes of the district, their geological situation, etc.—Elevation and depression of water in
the great lakes–Mean length, breadth, elevation and area of the several great lakes—
Elevation of the smaller lakes—Elevation of different points in the district from Lake
Ontario southward. - : -
The physical features of the district have already been alluded to at the commencement of
the volume; the principal valley of drainage is that of Lake Ontario, while the Susquehannah
and the Allegany are the outlets of a part of the waters of the southern portion of the dis-
trict. The north and south valleys, occupied by the Cayuga, Seneca, Crooked and Canan-
daigua lakes, with the lesser ones of Honeoye, Canadice, Hemlock and Conesus, are distin-
'guishing features of the district. These bodies of water, though small when compared with
the great lakes, are nevertheless of sufficient magnitude to claim our attention. They are all
situated in valleys of erosion; the rocky strata, with a slight dip to the south, appearing on
both sides. One of the remarkable features of this chain of smaller lakes is, that the four
406 GEOLOGY OF THE FOURTH DISTRICT.
first named, with several on the east of them, unite in one general outlet, the Oswego river,
and empty their waters into Lake Ontario. All these lakes, with the exception of the Cayuga,
are situated on the south of the great Helderberg series of limestones, which extend westward
from the Hudson river. The northern extremity of Cayuga lake valley is excavated in this
limestone, and in the Onondaga Salt group below. The greater part of these excavations have
been made in the rocks of the Hamilton group, the Portage group, and the northern portion
of the Chemung group. The small western lakes of this series do not extend so low as the
Hamilton group, as will be seen on reference to the Geological map of the district,
These bodies of fresh water exert a very sensible influence upon the temperature of the
surrounding country, and the effects of frosts upon vegetation bordering them is not observed
so soon by many days as on the higher grounds.
Cayuga lake, the most easterly of the chain, is nearly forty miles long, with an average
breadth of more than two miles. Its greatest ascertained depth is 390 feet. For several
miles before reaching its northern extremity, this lake is quite shallow, the bottom being dis-
tinctly visible; finally it is covered by aquatic plants, which reach the surface, and these
are succeeded by marsh grasses. The marshes have been before alluded to, and from their
immense extent are of great interest. The mode of reclaiming these by dykes, and by re-
moving the surplus water by aid of windmills, has been suggested in my annual reports, and -
it still appears to me practicable. Even during the warm summer months, there is almost
constantly a sufficient breeze upon these lakes to move a windmill; and after the first expense
of draining the surplus water from the higher grounds, it could be kept out by this method
with little trouble or expense. -
Seneca lake, the second in order, is of about the same length and breadth as Cayuga. Its
depth, however, is considerably greater, being five hundred and thirty feet. It does not become
shallow toward the northern end, as Cayuga lake. The outlet of this lake is evidently of more
recent excavation than that of the lake valley: it turns to the eastward, and joins Cayuga lake
near its northern extremity. It cuts its channel through the Corniferous limestone, and the
limestones and marls of the gypseous formation below.
The channels of both these lakes are very similar, and their valleys extend 'northward,
joining the great valley of the Susquehannah. Their banks are mostly perpendicular cliffs
of shale and sandstone, for a height of ten to sixty feet; and from this the country rises in a
gentle slope to a height of several hundred feet. This is covered with forest in its native state,
and when cultivated, forms some of the most beautiful tracts. The surface is indented with
ravines, which become deeper on approaching the lake shore, and open as deep gorges in
its perpendicular cliffs on the margin.
Crooked lake, is the third in the series. The aboriginal name of this lake is Keuka. Its
northern half consists of two branches, separated by a bluff of land, which rises, at its southern
extremity, more than three hundred feet above the lake. It appears to lie in a deepened por-
tion of a north and south valley, which northward joins the valley of Flint creek, and south-
ward the Conhocton at Bath. Its depth has been variously estimated; but from soundings
made at several points, the average is probably less than two hundred feet. The outlet is
LAKES. 407
lateral, and of very modern origin; emerging at Penn-Yan, and excavating a channel in the
lower part of the Portage group, the whole of the Genesee slate, and about two hundred feet
of the Hamilton group, it flows into Seneca lake at Dresden. The descent along this outlet
is two hundred and seventy-one feet. - -
Canandaigua lake, the fourth in the series, occupies a position in the rocks of the
Hamilton and Portage groups, extending northward almost to the Corniferous limestone. Its
length is about fourteen miles, and it has a breadth of from one to two miles. Towards its
northern end it is becoming shallow, and aquatic plants and grasses rise above the surface of
the water. There is also an extensive marsh at its southern extremity. This is the most
westerly lake that flows into the Oswego river. Its outlet is northward for several miles;
passing over the Corniferous limestone, and then turning eastward, it excavates a channel
through marl and gypsum beds of the Onondaga salt group. -
The three lakes, Honeoye, Canadice and Hemlock, lie in deep gorges in the rocks of the
Portage group. The first opens northward into a beautiful valley, along which the waters of
its outlet flow. The outlets of the other two unite, and after a circuitous route join that of
the Honeoye, which flows into the Genesee river. The length of the two largest of these
lakes is about six miles, and of Canadice about three miles. * -
The Conesus lake, of which a sketch is presented at the head of the chapter, is one of
the most beautiful sheets of water in the district. It is situated in rocks above the Hamilton
group, and presents gently sloping banks to the water's edge, covered with a fine forest of
oak, hickory, etc., except where the hand of industry has replaced them with cultivated fields
and meadows. Its length is about nine miles, with a width of one mile. Its depth does
not exceed sixty feet, and for the greater part is much less. Its outlet passes over rocks of
the Hamilton group, the Marcellus shale, the Corniferous and Onondaga limestone.
West of the Genesee valley, we find several small lakes in the higher rocks, and some of
them at great elevations above the ocean. The principal are Silver, J ava, Bear, Cassadaga
and Chautauque lakes. These are not situated in the well defined north and south valleys,
like those previously enumerated. Chautauque lake is the only one of any considerable mag-
nitude. It is eighteen miles long, and contains sixteen thousand acres. -
All the last named lakes, with the exception of Silver lake, flow into the Allegany,
mingling their waters with the ocean in the Gulf of Mexico. .
Of the chain of great lakes, we have to notice two as coming within the district: Lake
Ontario being the northern boundary, and Lake Erie, with the Niagara river, the western
boundary. They form two of those great depressions in the immense basin of the St. Law-
rence which are occupied by these seas of fresh water. The length of this basin or valley,
from the Gulf of St. Lawrence to near the sources of the Mississippi where it commences, is
almost two thousand miles ; and the whole area has been estimated at more than five hundred
thousand square miles, of which from eighty thousand to ninety thousand are covered with
water.”
* The area of this valley, and the surface of the water, are differently estimated by different individuals.
408 - GEOLOGY OF THE FOURTH DISTRICT.
The amount of fresh water contained in all these lakes has been estimated at ten thousand
five hundred cubic miles, being more than half the fresh water on the surface of the whole
globe. - . . . "
The basin of Lake Ontario is excavated in the Medina sandstone, the Grey sandstone, the
Husdon river group of shales and sandstones, and towards its eastern extremity in the Trenton
limestone. It appears probable, however, as stated by Mr. Vanuxem, that the Trenton lime-
stone forms the bed of this lake, its estimated general depth reaching to about the surface of
that rock. On its southern side the Clinton and Niagara groups of rocks rise in a high escarp-
ment, and the excavation from this point northward is doubtless due to the same cause which
eroded that portion now occupied by the lake. w -
The basin of Lake Erie is in like manner in the bottom of a deep valley of erosion; and
on its eastern and southeastern side, at the distance of four to eight miles, an escarpment of
the higher rocks rises to an elevation of from five hundred to eight hundred feet above the level
of the lake. It is quite evident that the strata, whose outcropping edges now appear on the
southeast of Lake Erie, once extended much farther to the north and west; and since there
is no evidence on the northern side of the lake of any sinking down of the strata, it would be
an unnecessary supposition to bring in any such agency to account for the existence of this
valley. . - - -
The Corniferous limestone forms the northern margin of this lake for many miles, and
dipping southward, probably forms its bed, as the small depth of the lake appears to indicate.
Had the eroding agency removed this limestone, the soft rocks of the Onondaga salt group
coming beneath would allow of a deep excavation with much less power than the limestone
above; and if this had occured, Lake Erie would probably have been the deepest lake of the
whole, while now it is the most shallow, - - -
Elevation and depression of the water of the Great Lakes.
The fluctuating level of the water of these lakes has long excited attention, and many
speculations have been hazarded to account for the phenomenon. The somewhat general
belief, that the periodical rise and fall in the water of these lakes occupy seven years, appears
not to be founded upon authentic observation. Sandbars and beaches, or the inlets to certain
bays, are regarded as the landmarks; and these being liable to fluctuation from accumulation or
removal, it follows that no hypothesis founded on such observations can be of any value.
Of this character were many of the early observations, where the harbors were entered
with a certain depth of water, which at some subsequent period was found to have diminished.
It is nevertheless true, that there are important fluctuations in the lake levels, which are
unconnected with the influence of winds. - - -
The only rational explanation of these changes yet offered, is that depending on the waste
and supply of water. From the immense surface exposed to the sun's rays, it is plain that
the amount of water evaporated is immense; and if by any means this process becomes re-
tarded, the water is elevated. Again, the greater quantity of snow falling during certain
LAKES. 409
seasons has been considered a sufficient reason for explaining this increased elevation of the
lakes. If after such a season, a summer follows when there is a small proportional degree of
sunshine, the amount of evaporation being thus diminished, the lakes remain at a higher point.
These causes, though perhaps satisfactory, and without doubt true, at least to a certain extent,
do not always appear sufficient to account for the fluctuations which have been noticed.
Twenty-five and thirty years ago the beach of Lake Erie was a travelled highway beyond
Buffalo, but at this time it would be quite impossible to travel along the same.
Though the removal of beaches of sand and pebbles may in some degree have modified
this line of coast, yet it is evident that the water now reaches several feet high upon rocky
bluffs, which at that time were beyond the reach of the waves. From the united testimony
of persons residing along the margins of all the lakes, and from other demonstrative proof, it
appears, that for many years previous to 1838, all the lakes had been rising; that about this
period they attained their maximum, and have since been subsiding. -
Mr. Hiram Burton, who has resided at the mouth of Slippery-rock-creek for twenty-three
years, informed me, in 1840, that the water of Lake Erie was then four feet higher than when
he came to that place; that in 1838 it was still higher, but he had made no accurate measure-
ments. This was estimated from the original position of a mill, which from the rise of water
had become useless. Several other persons who reside along this lake testify to the same
facts; and others, who travelled there many years since, agree in stating that the road from
Buffalo to Dunkirk was along the beach.
I have no means for determining the time or degree of the minimum depression of these
lakes. Mr. Higgins, topographer to the geological survey of Michigan, has given the rise of
the lakes as five feet three inches from 1819 to 1838; he regards it as probable that the
minimum period continues for a considerable length of time, while the maximum continues
only for a single year. In the absence of authentic observations, we can only rely on the
testimony before mentioned. This goes to prove that the lakes were at a low stage for twenty
years previous to 1819.
A single individual has informed me, that about the year 1788 or 1790, the lakes were
nearly as high as in 1838; and we have everywhere sufficient evidence that the water of the
lakes has, at some former period, been at a higher elevation than in 1838, and that subse-
quently it has been lower for a long period, previous to its last ascent. This evidence consists
in raised beaches along the lake shore, which have been left by the receding water, and upon
which trees have grown, and subsequently been undermined by the rise in the water. An
example of this kind, and perhaps the most satisfactory, is near Van Buren Harbor, on Lake
Erie. The water has encroached upon a line of beach, which borders a low ground, and
exposes a section of the same, which is composed of pebbles and lake sand, presenting in all
its characters and appearance the proof of its origin. After its formation the water subsided,
and it became covered with trees, which the water at the present time is undermining.
Numerous similar examples might be mentioned as occurring both on Lake Erie and Lake
Ontario; and after making all allowances for the fluctuating nature of the modern beaches,
[GEoL. 4th DIST.] 52
410 GEOLOGY OF THE FOURTH DISTRICT.
we have no other mode of explanation left than the one suggested. The existence of rocky cliffs
along the lake shores is likewise evidence of the same fluctuating elevation in the waters.
The annual fluctuations in the level of the lakes are doubtless due to the nature of the
seasons, depending on the quantity of rain and snow and the amount of evaporation. But
it is not so satisfactorily demonstrated that for a series of twenty years the quantity of rain
and snow has increased, or that evaporation was lessened uniformly throughout this period.”
The effect of winds in producing temporary elevations and depressions of these lakes is
very remarkable. A strong westerly wind will raise the water in the eastern end of Lake
Erie several feet in a few hours; a much larger quantity is driven down the Niagara river,
and although so rapid a stream below the falls, the water frequently rises fifteen or twenty
feet during a westerly wind. At the same time the water in the lake is diminished at the
western extremity, and a corresponding depression takes place. The prevalence of a strong
easterly or northerly wind, in the same way, drives the water to the western and southern
parts of the lake, and a much smaller quantity flows down the Niagara river during such a
period. The same effect takes place in a greater or less degree in all the lakes; the rising at
one extremity and sinking at the other, till the wind subsides, when it resumes its equilibrium,
and in so doing presents a beautiful exhibition of the long swells which are observed in the
ocean after the subsidence of a high wind.
The relative situation and elevation of these large and small bodies of water, with the rivers
and lakes of this and other parts of the State, have largely contributed to place New-York in
her exalted commercial relations with the surrounding country. The valleys of the Hudson
and the Mohawk have opened a passage through two ranges of mountains, by which the waters
of Lake Erie are mingled with those of the Atlantic, affording by the artificial means an easy
navigation from the one to the other. Again, the waters of the upper Hudson are turned into
the Champlain canal, on its summit level, and mingle with the Atlantic in the Gulf of St.
Lawrence instead of the Bay of New-York. The waters of the Tioga river are turned from
their natural course, through the Chemung canal; and instead of flowing by the Susquehannah
into the Chesapeake bay, now pass by Seneca lake into Ontario, and thence into the Gulf of
St. Lawrence. Far to the westward again, by the Illinois canal, the waters of Lake Michi-
gan are destined to mingle with the Mississippi. Man has here done much to accomplish all
these changes; but before man began, nature had done more, and to her are we indebted for
those facilities which no other portion of this or any other country enjoys. |
* I had collected some facts to prove that the former condition of the great lakes was, in some degree at least, influenced by the
elevations and depressions which have taken place along the eastern portion of our continent, extending sometimes as far as
these lakes. Other subjects, however, have so occupied my time, that nothing more than a crude hypothesis could be offered,
and therefore the subject is left for a future opportunity. -
In connexion with this subject, I have learned from the early navigators of the Hudson river, that forty years since, the influence
of the tides was not felt at Albany ; but since that period they have been gradually advancing, so that at present the difference
between high and low water is about two feet. This is alleged to have improved the navigation at some distance below Albany,
so that what were formerly difficult places to pass, now afford sufficient depth of water. This circumstance bears strongly upon
the modern accumulation of silt below Albany, which now obstructs the navigation at certain seasons. If from any circumstance
the tide has been gradually advancing up the river, the point of deposit of these light materials, being at the meeting of the
stream and tidal wave, would likewise take place at a higher point in the river. This is a subject of great interest, and as con
nected with the evidence of a former greater elevation of water in the Hudson river, is worthy of attention,
TABLES OF ELEVATION, etc.
TABLES OF ELEWATION, etc.
The following tables present the elevations, areas, etc. of the great lakes, and the elevations
of the principal lakes in the district.
TABLE of elevation, mean depth, length, breadth and area of the several collections of water
in the Great St. Lawrence Basin.”
|-
Q} ... +:
53 # #
*: rd ..& .# •
; ## º: : : # AREA.
ÉÉ § # §§
- Feet. Feet. Miles. Miles Square miles.
Lake Superior,--------------- 641 900 300 80 24,000
| Lake Huron, ---------------- 596 900 200 95 19,000
Lake Michigan, --------------| 600 900 300 50. 15,000
Lake Erie, ------------------| 565 120 230 35 8,030
Lake Ontario,----------------| 231 492 180 30. 5,400
River St. Lawrence and smaller | . .
lakes, - - - - - - - - - - - - - - - - - - - -l- - - - - -,-,-l. 20 ... ... • * * * * *.*, *.ſ as mºsº.'s sm. flºº. ºx tº 1,500
Total water surface, -----|---------------- mº sm--sºº gº sº tº º- gº sº ºm º ºs tº mº sº wº 72,930
* From Prof. J. HENRY's Topographical Sketch of the State of New-York. Transactions of the Albany Institute, Vol. 1.
52*
AI2 (SEOLOGY OF THE FOURTH DISTRICT,
TABLE of the mean length, breadth, depth, elevation and area of the Great Lakes and the
- River St. Lawrence.”
# .d § 3
# # gº à
# =# º ### AREA.
§ § 3; § 5 §§
> E 5 > § 3 ;
Miles. Miles. Feet. Feet Square miles. ||
| Lake Superior--------------- 400 80 900. 596 32,000
| Green Bay, ----------------- 100 20 500 578 2,000
Lake Michigan,-------------- 320 70 1,000 578 22,400
Lake Huron, ---------------- 240 80 1,000 578 20,400
Lake St. Clair,<-------------- 20 18 20 570 360
Lake Erie, ------------------ 240 40 84 565 9,600
Lake Ontario, --------------- 180, 35 500 232 6,300
| River St. Lawrence, -----------|--------|-------- 20 -------- 940
| - ! - 94,000 |
It will be perceived that there are some differences in the two preceding tables; and not
having the means of deciding the absolute truth, both are given. These are to be regarded
as an approximation to the truth, rather than as absolutely correct.
The following are the elevations of the principal lakes within the district.
| Above Lake Above tide
Ontario. water.
- - - Feet. Feet. ſ
Cayuga lake, ------------------------- 156 387 |
Seneca lake.-------------------------- 216 447
Crooked lake, ------------------------ 487 718
Canandaigua lake, --------------------- 437 668
Chautauque lake, ---------------- tº ºne ºn emº ºm sº 1,060 1,291
The elevation of the other lakes is not known with sufficient accuracy to give them in this
table. -- *
The three following tables of elevations, from the paper of Prof. Henry before quoted,
present three lines of section in a north and south direction across the district.
* Report of Dr. Houghton, State Geologist of Michigan.
TABLES OF ELEVATION,
413
etC.
TABLE of ascents and descents from Great Sodus Bay, on Lake Ontario, along Seneca lake
and the route of the Chemung canal, to Newtown on the Chemung or West Branch of the
Susquehannah river.
\
ROUTE. Miles Feet,
Lake Ontario, at Great Sodus Bay,-----------------|----- - I - - - - - -|------------| 231
Lyons, on the Erie canal,-------------------------|------ 15 Rises 170 | 401
Outlet of Seneca lake, near Geneva, ---------------- 12 27 Rises 46 || 447
Along the lake to its head, ----------------------- 34 61 Level,----- 447
Summit between the lake and Chemung river, ------- |-| 8 69 Rises 443 | 890
The Chemung at Newtown,----------------------- 10 79 Falls 53 | 837
TABLE of ascents and descents from Lake Ontario, along the valley of the Genesee river, to
the mouth of Black creek in Allegany county, and thence to Olean on the Allegany
river, along Oil and Black creeks.
ROUTE,
| Mouth of Genesee river, ----------------------------
Erie canal at Rochester, ----------------------------
Squakie hill, ------------------------------------
Gardeau flats, -------------------------------------
Head of the great falls, Portage, --------------------- &
Mouth of Black creek, ----------- ------------------
*Summit level between Black and Oil creeks, -----------
Olean on the Allegany, --------- •ºg ºss tº Ei ºl º ºsº º ºs gº tº - - - - - - - ** = ºl
Miles Feet
* * ſº tº gº ºne i ºs sº smºs º º -|------------| 231
sº ms sº tº ºne ºr 8 Rises 275 506
29 37 Rises 68 574
6 43 Rises 76 650
8 51 Rises 453 | 1,103
16 67 Rises 162 1,265
10 77 Rises 221 | 1,486
13 90 Falls 78 || 1,408
ld
TABLE of ascents and descents from the mouth of Oak-orchard creek on Lake Ontario, in
nearly a direct line to Olean on the Allegany, by the route of Batavia, the Tonawanda
creek, Lime lake, and the valley of Ischua creek.
Z
ROUTE. Miłes Feet
Lake Ontario, at the mouth of Oak-orchard creek, ------|------|----- - | | * * * * * = - - - - - - 231
| Albion, on the Erie canal, --------------------------|------| 8 #ises 275 506
Tonawanda creek, at Batavia, ----------------------- 17 25 Rises 77 883
Attica, along Tonawanda creek, ---------------------| 11 36 Rises 571 954
Dividing ridge between Tonawanda and Cattaraugus creeks, 18 54 Rises 426 1,480
Lime lake, ---------------------------------- -----| 14 68 Rises 143 1,623
Olean point, on the Allegany, along the valley of Ischua
and Oil Creeks,--------------- * * * * * * * * * * * * * * * * = m, em. 27 93 Falls 214 | 1,409
* This summit is a marsh, the discharged waters of which find the level of the ocean in the Gulf of St. Lawrence and the
Gulf of Mexico.
414 GEOLOGY OF THE FOURTH DISTRICT,
CHAPTER XXII.
Local Geology and Economical Products of the Counties comprising the Fourth
Geological District. -
[The details of this chapter have been chiefly extracted from the Annual Reports of the District.]
wAYNE COUNTY.'
The rocks of this county consist of the Medina sandstone, Clinton group, Niagara group,
and the Onondaga salt group, ranging in nearly an east and west direction throughout the
county. In the eastern part of the county the Medina sandstone forms but a narrow belt
along the lake, but gradually expands towards the west. The other groups follow in succes-
sion. The best lines of exposure are from the Wolcott furnace southward along the creek;
at Whiting's mill, about three miles further east; at Sodus bay, and in Ontario. The Clin-
ton group presents some interesting features in this county which have not been observed far-
ther eastward; and the geologist will find the Wolcott ore-bed, the creek at Wolcott's furnace,
Whiting's mill, the former Shaker settlement, and the town of Ontario, interesting localities
of these rocks, their minerals and fossils. -
South of the Ridge road the country is occupied by numerous long, narrow and parallel
ridges, rising from twenty-five to thirty-five feet above the general level, and having uniformly
a north and south direction. The ridges are composed of sand and gravel.
They extend regularly as far north as the Ridge road, where they all terminate. This
was observed particularly in the towns of Sodus, Williamson, and Ontario. We saw no
instance in which these ridges cross the Ridge road,i On the old Sodus road we travel north-
ward, for about a mile, between two of these parallel ridges, which are here quite as high as
any in the county, when, upon descending a little towards the flat country, they terminate,
and here a continuation of the lake ridge connects the points of these ridges or hills. This
place is about half a mile south of Griffith's tavern, in the town of Sodus. From this point
to the lake, the country is a gradually descending plain.
*The details of this county are principally from the Report of the late Dr. G. W. Boy D. (Ann. Rep. of the District for 1838).
f This circumstance is referred to particularly, because the fact is important in considering the origin of the lake ridge.
WAYNE COUNTY. - 415
The ridges about Clyde, and generally in the town of Galen, north of the canal, are nume-
rous, long, narrow, low, and have a north and south direction. -
Ridges in Lyons are also long, narrow, and low ; both sides and top are cultivated.
The only exceptions to the northerly direction of the ridges were noticed in the town of
Walworth, near Walworth corners, where there are two or three east and west ridges, upon
one of which the village is situated. These form the highest land in this part of the county,
between lake Ontario and the Erie canal. Also, in the town of Macedon, between the centre
and the Erie canal, the country is broken, and the hills irregular.
The lake shore in Wayne county is generally bold, and composed of a bank greatly vary-
ing in height. About the mouth of Salmon creek it is ten feet high ; at Pultneyville, in the
town of Williamson, about eight feet; at Sodus Point, from eighty to one hundred feet.
The bank is composed of sand and gravel, with occasional layers of clay. Generally a beach
of some width runs along the shore, varying from fine to coarse gravel, according to the state
and direction of the winds; it is sometimes entirely swept away by the excited waves of the
lake. | - -
In Wayne county, the Erie canal is carried along the valley of the Clyde, from both sides
of which the country takes a very gradual rise. Canandaigua, Crooked, Seneca, and Cayuga
lakes discharge their waters northwardly into the stream which traverses this valley. The
stream is known first as Mud Creek, until joined by the Canandaigua outlet, when it becomes
Clyde river, and so continues eastward as far as Montezuma, where it receives through the
Seneca outlet the waters of Crooked, Seneca, and Cayuga lakes, and then continuing east
through Cayuga into Onondaga, joins the outlet of Oneida lake, with which it forms the Os-
wego river. The latter finally empties all the waters of the Clyde and Oneida valleys, in-
cluding fifteen lakes, into Lake Ontario. -
It was suggested to me by Col. Elias Cook, of Sodus Point, that at a former period, and
perhaps previous to the formation of the Cayuga marshes, the Seneca river discharged a
part or the whole of its waters northwardly through the towns of Butler and Wolcott in
Wayne county, along the Wolcott Creek” into Port bay on Lake Ontario. An examination of
the country renders this opinion very probable. The marsh extends past Crusoe lake, which
is immediately north of the island of the same name, into the town of Butler, to within a
short distance of Wolcott creek. Also, by the surveys of Col. Cook, it appears that the
rock in Wolcott Creek at Marble's quarry (lot 165 in Butler), is only one foot above the level
of the Montezuma marshes. This is a distance of about six miles, and the excavations would
be through sand and gravel. The extensive water-worn surface of rock in the creek at Mar-
ble's quarry, indicates the passage of a much larger body of water than is now transmitted
through this channel. At the village of Wolcott, we also notice a large gorge or gulf, pro-
duced by the current of a great body of water along the course of the present stream. The
creek at present falls over the eastern part of this gulf; and upon no occasion of freshet in
the present stream, does the water extend to the other side of the gulf.
*Its proper name is Mill creek,
416 GEOLOGY OF THE FOURTH DISTRICT.
Marshes and Swamps.
The Cayuga marshes occupy a part of the town of Savannah, surrounding both sides of
Crusoe island, and extend beyond Crusoe lake into the south part of Butler. These marshes
contain a deposit of calcareous marl, apparently equal in extent to that of the marshes. The
Erie canal is cut through them for several miles, and penetrates the marl to the depth of five
or six feet. This marl contains abundance of freshwater shells.
One mile west of Newark, a bed of shell marl appears in the banks of the Erie canal. It
is whitish, and contains shells similar to the preceding. The depth of this bed is unknown,
but it is probably small. It extends about one mile along the course of the canal.
In the south part of the town of Williamson, at Cooper's swamp, is a thin bed of whitish
marl, containing shells similar to the preceding.
The calcareous marl above mentioned consists principally of carbonate of lime, with a lit-
tle vegetable matter, and is in an earthy or friable state, perfectly adapted to employment as a
manure. We are not aware, however, that it is at present applied to any useful purpose; but
we conceive that it is equal in value to our western plaster, and may be a better application
to some lands. We would suggest to the intelligent farmers in the vicinity of the Cayuga
marshes, who may penetrate this marl in the course of ditching, to make a comparative trial
of this article with the neighboring plaster.
A cranberry swamp was noticed at the head of Port bay, about three miles in length and
one and a half in breadth ; it shakes, is movable, and at times an acre or more has become
detached and floated into the water.
Boulders.
Primitive boulders are noticed in abundance in Wayne county, but they do not occur of a
large size; they seldom exceed half a ton in weight. Some of them could be distinguished
as of similar character to rocks in the northern counties of the State ; and among all the er-
ratic masses which I have noticed, none were considered to be of southern origin. A great
variety of primitive boulders occur in and about the village of Clyde; also in the town of
Butler.
Soil.
South of the ridge the soil consists of a sandy loam, lightest, as the farmers say, on the
west side of hills, and strongest and best on the eastern sides. This may be owing partly to
exposure, and to the circumstance that the western sides of hills are frequently bared of snow
by the westerly winds of winter. Beach, maple and bass-wood generally prevail on the east
sides of hills, and hemlock on the west. North of the ridge, the surface is decidedly more
sandy; yet in Wolcott and other towns in the south part of the county, the soil is generally
productive, and the crops are good: it is a grain-growing country.
WAYNE COUNTY... . 417
Mineral and other waters.
The springs in this county arise chiefly from limestones, or from shales and marls, which
contain a proportion of lime ; of course they are more or less impregnated with calcareous
matter. Along the lake, however, the sandstone range furnishes springs of a pure and soft
Water. - - y -
Sulphur Springs.
Several sulphur springs arise in Brown's mill pond, about one and a half miles south of
Newark. The water running from this pond deposits sulphur, and sulphuretted water issues
from the bank at the road opposite the dam, and forms a whitish deposit. When the water
in this pond becomes low, the small fishes which it contains are sometimes found dead, floating
on the surface. No other cause than the properties of the sulphurous springs has been as-
signed for this fact. - - - - wa
On Salmon creek, near the forge in Sodus, a weak sulphurous spring rises from the red
sandstone, and forms a reddish deposit. One or two sulphur springs also occur in and near
Palmyra. At Jenkins's hill, in the village of Clyde, there is a weak mineral spring, proba-
bly of a sulphurous nature. With the exception of that on Salmon creek, all these springs
occur in gypseous rocks. About half a mile northeast of Marion Centre, a sulphur spring
rises from the bituminous limestone. This place is resorted to by residents of the vicinity,
and occasional visiters. -
Salt Springs.
The old Galen salt works are situated on lot No. 54 in the town of Savannah, immediately
on the western edge of the Cayuga marshes. The spring is large, and is indeed quite a
pond of perhaps twenty feet in diameter. Salt was manufactured about twenty-five years
since, when the country was new and but thinly settled.
One or two salt springs formerly appeared in the creek, a short distance below Wolcott fur-
nace; they are now neglected and filled with fresh water. These springs were worked in
1815, and furnished a reddish salt. They rise from the red sandstone. Another salt spring
rises from the red sandstone upon a small creek emptying into Sodus bay, near the point.
Two miles east of Lockville, near the Erie canal, boring was made for salt. There was
originally a spring at this spot, and salt was manufactured to a small extent. -
Deep boring for Salt Water at Clyde.
In 1832, a company bored to the depth of 400 feet in the immediate vicinity of Clyde.
The spot selected had no indications of a saline or other mineral character, and there was no
spring; the boring was commenced in the gypseous rocks. Salt water was obtained in
small quantity, but quite strong. A square wooden tube now projects several feet f: the spot
[GEoL. 4th DIST.] 53
4|8 GEOLOGY OF THE FOURTH DISTRICT.
where the boring was made, but at present the water does not rise to the surface. Gypsum
was found at the depth of twenty-five feet, which continued at intervals for 100 feet; below
this was found sandstone, and occasional hard layers of rock—towards the last, so hard that
the drill gained only an inch per diem. They passed through a fissure at 100 feet. Salt or
brackish water appeared at 170 feet. The lowest rocks were sandstone and slates. Inflam-
mable air was discharged during the boring, and also subsequently. At the time of our visit,
on shaking the wooden tube, a gurgling noise could be heard below ; and then upon passing
down a burning paper, an explosion took place in the tube. No decided Odor could be distin-
guished. Doubtless this inflammable air was carburetted hydrogen, as it has been frequently
noticed in the Western States in similar borings for salt. Messrs. Reese and Stowe were of
the company who made the search, and from them we received the preceding account of the
work; the former gentleman presented us with the only sample he then possessed of the
rocks penetrated during this boring, and which was extracted from the depth of 348 feet,
Clay, suitable for the manufacture of brick, occurs abundantly along the line of the canal,
and in limited beds at several points near and north of the ridge. -
Gypseous Marl.
Plaster marl (the local name) occurs at many points on the Erie canal, and extends south
into the adjoining county of Ontario. It generally appears as a soft slaty rock, or as an in-
durated marl, of an ash grey, and sometimes a greenish color. It is the gangue of the gyp-
sum or plaster, in this, as well as in the neighboring counties. This marl generally contains
an appreciable proportion of lime, although in some instances it is entirely argillaceous. Al-
though of the nature of solid rock when first extracted, upon exposure to the air it slackens and
crumbles down in a short time. We are not aware that it is used as a manure, but without
doubt to sandy soils its addition would be very profitable, perhaps as much so as the plaster
which it affords; inasmuch as soils purely sandy require clay as well as lime to give them a
proper character of composition.
Near Clyde, the gypseous marl is seen of a dark grey color, slaty.structure, and contains
marine fossils, among which are Orthocerae, Trilobites, and a variety of shells.
At Lockville, one mile east of Newark, it occurs, greenish, reddish, and variegated, in the
banks of the canal, and in various excavations, especially at a race-way from Price's mill.
At the latter place I examined and collected the marl. The greenish variety is amorphous,
and contains gypsum in irregular or curious crystals. It effervesces with acids. Another
variety is slaty, grey or ash color, soft, penetrated by numerous very thin seams of gypsum,
and does not effervesce with acids. It appears to be entirely argillaceous, slackens upon ex-
posure to air and moisture, and crumbles to a dry earthy powder.
WAYNE COUNTY. 419
Bog and Argillace0us Iron.
About one mile east of Lockville, bog iron occurs, covering about an acre; it is in large
solid masses near the surface, and is frequently turned up by the plough.
A stratum or bed of argillaceous oxide of iron extends through Wayne county, parallel to
and at the distance of about two miles from the lake. Furnaces for the reduction of this ore
have been constructed in the towns of Wolcott, Sodus and Ontario. It has been ground for
paint, and hence receives the name of paint ore. It belongs to the lenticular variety of mi-
neralogists. It is always accompanied by greenish argillaceous shales and thin layers of shell
limestone, and the ore itself seems to be composed chiefly of marine shells and other fossils,
similar to those in the shales and limestones above and below.
The argillaceous ore makes a hard, brittle iron. When melted without any flux, it is too
sharp, i. e. the cinder is equally as fluid as the iron, from which it does not separate, but will
sometimes run to the end of the mould. The melted mass is too thin, and therefore it is ne-
cessary to mix loam with the ore. At the Wolcott furnace, Mr. Hendrick uses one part of
sandy loam to two parts of ore, upon which the cinder separates, and perfect castings are pro-
duced. Mixed with the rock ore, or magnetic oxide from Canada, in equal parts, and also in
the proportion of two parts of argillaceous to one of magnetic ore, a softer and better iron is
produced. - -
The argillaceous oxide requires a high heat for melting, and consumes one-third more char-
coal than the harder ores. There is always produced considerable carburet of iron in thin
bright scales or leaves, exactly resembling plumbago; we have also seen this substance formed
from the magnetic ores of iron at a high heat. -
When casting plough irons, they run them upon a hardener (which is a piece of cold
iron), so that for two inches on the edge, which is liable to wear, the castings are hardened
like steel. The effect is, to change the usual granular texture of the casting into one that is
lamellar, like bismuth. This difference is perceptible, and the line of demarcation is also -
very evident when the casting is broken. -
Ontario furnace is situated upon Bear creek, about two miles north of the ridge. The ar-
gillaceous iron ore is extracted in two places in the immediate vicinity of the furnace; it
is a continuation of the same stratum that is explored in the towns of Sodus and Wolcott.
The layer of iron ore is situated about fifty feet above the surface of Lake Ontario. Solid
ore occurs about three feet thick, and to a greater extent mixed with rock; it is clean, of a
bright red color, exhibits its fossils very distinctly, and its characters are generally simi-
lar to those of the Wolcott ore. It is said to yield from 33 to 35 per cent of metallic
iron. The iron which it forms is brittle, and is employed for large castings, as potash kettles,
ploughshares, etc. Bog ore improves it. The ore is quarried and delivered at the furnace
for $1.50 per ton. There were formerly manufactured at this furnace 300 tons of iron per
annum. This ore was first dug during the last war, carried to Auburn, and ground for paint,
of which it is said to form a good article with the addition of a little red lead.
53*
420 GEOLOGY OF THE FOURTH DISTRICT.
Quicklime.
The Niagara limestone runs in an east and west direction across Wayne county, through the
towns of Butler, Rose, the lower part of Sodus, Marion and Walworth, upon which are situ-
ated a line of kilns, which furnish an ample supply of lime of an excellent quality. The
limestone is frequently of a dark color, and contains bitumen, which is, however, expelled
in the process of burning, and a white lime is produced. -
Hydraulic Lime.
One mile south of Newark there occurs a grey sandy limestone of a slaty structure, which
resembles the hydraulic limestone of Onondaga county. Also, in the south part of Williamson
there appears a slaty, siliceous limestone, similar to, and in the same range with the hydraulic
limestone of Monroe county. The Williamson rocks are immediately under the Niagara
limestone mentioned under the head of Building stones, while those near Newark are above it,
and also superior to the gypsum. A similar rock occurs at Merrick’s mill on Van Awken’s
creek, in the town of Rose. -
Firestones.
Limestone, containing an abundance of shells and other fossil remains, is generally employed
in this county for hearth stones, and in other situations exposed to frequent changes of tem-
perature. Such stone occurs at Merrick's mill, in the town of Rose; in the town of Sodus,
south of the ridge, and in other parts of the county, in the range of shale under the Nia-
gara limestone. ,
The range of sandstone in this county is narrow, not exceeding two miles in width, and lies
immediately along the lake shore. It does not appear to be used for architectural purposes;
indeed, it is too soft, slaty and argillaceous, except in the town of Wolcott, where the upper
layers are hard, siliceous, and occasionally pass into conglomerate or puddingstone. These
upper layers have been quarried and used in the construction of furnaces, as at Wolcott. At
the forge on Salmon creek, the sandstone contains abundance of the Fucoides Harlani. -
The sandstones of Beard's creek and Little Red creek, in the town of Wolcott, endure the
action of heat sufficiently well to answer for side stones of furnaces, and they are employed
for that purpose at Wolcott. When exposed to a red heat, and beyond that, they do not ex-
pand; on the contrary, they appear to contract, so that when used for the hearth, the temp
stone (which is like the key stone of an arch) has sometimes fallen out. -
At the Wolcott furnace, at present, they use and approve of the Oswego stone, viz. the
red sandstone of Oswego falls, which is a part of the same formation as this in Wayne. The
Oswego stone expands upon being heated, and is therefore well adapted for hearth stones.
At the glass-house in Clyde, they have employed the Haverstraw sandstone; but they now
use, in preference, the stone from Perryopolis, Penn., and from Vienna, Ontario county.
WAYNE COUNTY. - 421
Building Stones.
The range of limestone that we have referred to under the head of Quicklime, passes through
this county about midway between Lake Ontario and the Erie Canal, in an east and west di-
rection, having a width of from two to three miles. Many favorable situations occur for the
extraction of building stone of an excellent and durable nature. This rock varies in color
from light to dark blue, is of a granular texture, sandy, and emits a bituminous odor on
percussion. It occurs in layers, of from one to three feet in thickness, having a horizontal
position, and an elevated and dry situation. - - --
Uttoe's qr Miner's quarry, lot 132 in Rose, is on the head waters of Sheldon's creek. The
rock occurs in extensive layers, two or three feet thick, of a dark blue color, granular texture,
and highly bituminous. This quarry has furnished an approved stone, which was employed
in the locks of the Erie canal, at Clyde. -
Henderson’s quarry, lot 141 in Butler, affords large blocks of a building stone, similar in
all respects to that last mentioned. -
Roe's quarry, in Butler, furnishes a dark compact limestone, which is bituminous. It is
employed in building, and also for the manufacture of lime, of which it affords an article of
excellent quality. It is a magnesian limestone, and contains only a few fossils, among which
we recognize Cytherina. - - . . .
A compact shell limestone, which occurs near the Shakers’ mill in Sodus, is quarried as a
marble, and used for ornamental purposes. - - - -
Gypsum.
The range of gypseous rocks extends on both sides of the Erie canal, along the southern
part of Wayne county, but generally lies too low for profitable exploration. At Clyde, gypsum
is found in wells at the depth of twenty-five feet. In wells at Lyons it has been found at
forty feet, and also in Palmyra, at about the same depth. - r
About two miles west of Newark are two hills, from which gypsum is quarried. At this
locality it is mostly lamellar, transparent, and receives the local name of isinglass plaster.
422 GEOLOGY OF THE FOURTH DISTRICT.
MONROE COUNTY.
The rocks of this county are the same as those in Wayne county. The Niagara group,
however, becomes better developed, and its fossils more numerous. The Medina sandstone
expands to a greater width, bordering the lake shore. The Clinton group perceptibly dimi-
nishes in thickness, and its most prominent fossil, the Pentamerus oblongus, disappears
before leaving this county. The Onondaga salt group seems even better developed than in
Wayne county, and its numerous beds of gypsum are more extensively exposed. The course
of the Genesee river affords the best section of these rocks, and is quite sufficient to give one
an idea of the position and nature of the strata without visiting any other place.
Surface of the Country, Streams, &c.
The general elevation of the northern part of this county is about three hundred or three
hundred and fifty feet above Lake Ontario. All that portion of the county south of the canal
maintains about this elevation, if we except the drift hills, which rise to the height of from
fifty to one hundred feet. On the north of the canal the surface declines gradually, and
almost imperceptibly, to the lake shore; on the east side of the Genesee being more uneven
than on the west. In the northern part of the county, particularly north of the Ridge road,
the surface is remarkably even. We here find scarcely an undulation or depression disturb-
ing the uniformity, except the channels of the present streams.
East of the Genesee, particularly in the vicinity of the Irondequoit creek and bay, the
country is very much broken into deep ravines and high ridges. The ridges are com-
posed chiefly of fine sand, or sandy loam, with strata of pebbles or boulders near the
bottom. Most of the boulders in these hills are from the rocks in the vicinity, those of the
primitive rocks being comparatively few in number. In this and some other respects, the
drift along the Irondequoit differs from that of any other part of the county. There have
been vast accumulations of diluvial matter about the head of Irondequoit bay, and along its
shores. It appears as if at one time this had been a great water-course, and that some inun-
dation of sand, gravel, etc. had filled it up, and changed the direction of the stream. The
sand of these hills is stratified, and the strata often curved, or inclined at different angles.
The banks of the bay are high, with deep ravines scooped out by the action of the smaller
StreamS. - - k
The bed of the Irondequoit at Penfield, is much lower than the bed of the Genesee at Ro-
chester and farther south. From examining the surface of the country, this seems the most
natural course of the Genesee, and it may at one time have flowed in this channel. The
Irondequoit is now a small stream, pursuing its course in a deep valley of denudation, show-
ing that some more powerful agent was formerly active in this quarter. -
MONROE COUNTY. 423.
Farther south and distant from the streams, through the towns of Penfield, Perrinton, Men-
don, etc., the drift hills are of moderate elevation, giving a gentle undulating appearance to
the country. In the south part of Perrinton the surface is very irregular, the hills rising
from fifty to one hundred feet above the general level. These are composed of gravel and
hardpan, and the general character of the soil is gravelly. Some of the hills are sandy, sup-
porting a growth of shrub oaks and whortleberry; the soil, however, is said to be good when
reclaimed. West of the Genesee, few hills rise to a greater height than thirty or forty feet.
All those in this part of the county rest upon the gypseous formation, and many of them
are formed by the destruction of the upper portions of these strata.
Most of the streams afford eligible mill seats, and it is to the water power furnished by the
Genesee that Rochester owes much of her prosperity. The great accumulation of water
power at that place, depends on the geological structure of the country. Had all the strata
been of equal hardness, the grand and beautiful succession of falls and rapids would not have
been produced, but in place of them a uniform, rapid current to the lake.
The Mountain ridge, or “limestone ridge,” so called, becomes well defined a few miles
west of Rochester. Here its elevation is only fifteen or twenty feet, but it gradually rises
towards the west, and at the western line of the county is forty or fifty feet above the level of
the country on the north. This ridge or terrace does not pursue a direct line, but is tortuous
and irregular in its course. - -
In many places we find swamps or marshes with large accumulations of partially decom-
posed vegetable matter, though none of it has yet become peat. The substance is usually
termed “muck,” and is used in some places as manure. There are several of these swamps
along the lake shore, where immense quantities of “muck” are deposited. Others on the
south side of the ridge road, exhibit finely comminuted vegetable matter, with trunks of trees,
deposited, often to the depth of several feet. The trees growing in these swamps are com-
monly black-ash, tamarack, and cedar. In the southern part of the county are several swamps
of this character, where the vegetable matter covers a deposit of shell marl—both substances
of great value as manures.
Lake Shore.
The lake shore of this county is for the most part low, the land gradually declining to
the level of the water. The action of the waves, together with the ice, have raised beaches,
which in many places protect the land from inundation during high winds. In the eastern
part of the county, the banks are abrupt, consisting of gravel, sand and clay. These banks
are gradually worn away by the waves, and the materials carried to points where the banks
are low. By this wearing action the lake encroaches upon the land in some places, while
the land is gaining upon the lake in others. In the course of a year, several feet of these
banks are abraded by the waves. The wind from the northeast carries the abraded materials
towards the mouth of the Genesee, and thus aids in filling up the channel, and extending the
shoals and sand-bars in the vicinity. The shores being low on the west of the Genesee, a
424 GEOLOGY OF THE FOURTH DISTRICT.
west or northwest wind brings few materials from that quarter. When the lake is higher
than usual, even the low beaches are worn down, and the materials transported to other parts
of the shore.
The bank of the lake, from the Genesee river to the eastern boundary of the county, is
from ten to thirty feet high. From the Genesee to the western line of the county, the shore
is generally low, or raised into a beach a few feet above the lake. During the rising of the
lake, which occurs at intervals, the beaches and sand-bars are removed, to be deposited in
other places, and to fill up the mouths of streams. It therefore becomes a matter of import-
ance to protect the shores from such effects, and from the loss of land thus sustained. To do
this, trees and shrubs should be permitted to grow on the banks, and shrubs with strong
roots might be planted to effect the same object. r
Boulders—Erratic Blocks.”
Boulders of different rocks are abundantly distributed over some parts of the county. They
are most abundant north of the mountain ridge, and over the gypseous rocks in the south part
of the county. In many places the surface is literally covered with them for a considerable
extent, and again for a mile or two few are seen. These boulders are of the primitive rocks,
as granite and gneiss, and of sandstone from the lower formation. Granite and sandstone are
the prevailing boulders, but rounded and angular fragments of rocks of every formation, in the
district, are found on the surface, some of them immediately above the original rock, and others
at no great distance from it. The predominance of felspar is observed in all the granite
boulders; many of them being of that variety called Labrador felspar. This felspar is very
indestructible, and masses of that rock form some of the largest boulders in the county.
Some of the spherical masses are eight or ten feet in diameter. These are in many places
so abundant as to be broken up and used for building materials.
Soil.
The prevailing soil of Monroe county is a gravelly loam; but we often find clayey loam,
sand, etc. extending over considerable areas. Approaching the Genesee river on either side,
the soil is more sandy; this character prevails, also, along the Irondequoit. In some places
the different soils blend into each other, and in others are quite distinct, or their limits are
defined by the small streams. Sometimes changes of this kind are remarkable, where on
crossing a stream the character of the soil is entirely different. The sandy soils are not defi-
cient in carbonate of lime, and the sand from several feet below the surface is apparently as
* We cannot, with propriety, restrict the term boulder to a rock distant from its original ſormation; for in the southern part of
the State, rounded masses of the red sandstone are boulders; while masses of the same form are found on the limestone a few
rods south, and in the soil above the original rock, which by that definition are not boulders. f
MONROE COUNTY. - 425
fertile as the original soil. Some of these sands require the addition of aluminous matter, to
render them of proper consistence for retaining moisture. . .
Where there are no disturbances in the surface from streams or other causes, the character
of the soil depends much upon that of the rock beneath; but owing to such causes, we
cannot safely depend on this criterion. The upper strata of the sandstone produce a
sandy soil, but its character is modified by the decomposition of the shales above, which
generally supply sufficient argillaceous matter. The marl of the sandstone formation below
the upper strata, produces a loamy soil, in some cases approaching to clayey loam. Sometimes
this soil is mixed with gravel or sand, and no one kind prevails over an extensive district. It
is no uncommon occurrence to find, in the same field, sandy, clayey and gravelly soil. The
soil on the north side of the lake ridge, for the most part, is more uniform in character than
on the south. That on the north side requires more care and labor in the cultivation, but is
thought to produce quite as good crops as the soil on the south side. Wheat, in some instan-
ces, has been sown on these soils ten years in succession. The soil above the sandstone has
often a brownish color, arising from the character of the rock beneath.
The shales above the sandstone produce a clayey soil, which, however, contains a sufficient
quantity of carbonate of lime to render it extremely fertile. The soil produced by the de-
composition of the shale, north of the mountain ridge, is perhaps the most productive of any
in the county. It is peculiarly adapted to the growth of wheat; but if tilled for a long time, and
particularly if worked while wet, it becomes “stiff,” and hard, like clay. - • , -
Clays might be used, to manifest advantage, on some of the sandy soils, particularly in the
eastern part of the county, where the same farm often contains both sand and clay.
The soil upon the limestone is from a few inches to twenty feet in depth, of a loamy cha-
racter, and very fertile throughout. The slow disintegration of the limestone affords a suffi-
cient proportion of carbonate of lime; and if vegetable matter be also furnished, the soil will
not soon be exhausted. In the southern part of the county the soil is gravelly or sandy on the
hills, and clayey in the valleys and low grounds. It contains a large proportion of carbonate
of lime, arising from the decomposition of fragments of slaty limestone which are distributed
throughout. In some places we find extensive deposits of coarse gravel, with boulders.
Clays.
The clays of Monroe county are of that kind fit for bricks and the coarsest kinds of pot-
tery. The varieties are grey, blue and brown clays: grey and blue varieties prevail along the
lake shore; those in the interior of the county are brownish or variegated. Every part of
the county furnishes beds of clay of greater or less extent, but the demand for bricks has been
limited to a few points. As many as five or six beds of clay have been wrought in the vici-
nity of Rochester, from which about 2,000,000 of bricks are furnished annually. Bricks
have been made near the village of North-Penfield, and there is an extensive deposit of clay
on the lake shore in the north part of the town of Brighton. Bricks are made near Fairport,
[GEoL. 4th DIST.] 54 -
426 GEOLOGY OF THE FOURTH DISTRICT.
and at Mendon and Pittsford. Beds of clay occur near Clarkson and Brockport; from some
of which, bricks have been made. We might enumerate every town in the county, but the
materials are similar, and are found in all.
The decomposing gypseous marls appear at the surface in Pittsford, and other places, where
they have been mistaken for clay. This marl contains too much carbonate of lime to be use-
ful for bricks, but would be valuable if used as a manure on sandy lands. It makes bricks
of a very inferior quality, which crumble on exposure to rains, and are peculiarly unfit for
exposure to water. - -
Sands.
The only pure siliceous sands we find in this county are on the lake shore. With these,
garnet and iron sands occur in small quantities. Coarse sand or fine gravel, fit for making
mortar, is found in many places, particularly along the Irondequoit, and in many of the drift
hills. The fine sand of these hills contains too much argillaceous matter to be useful where
a siliceous sand is required. At the outlet of the Irondequoit bay, great quantities of a
pure siliceous sand is drifted into ridges along the shore. Sand may be obtained from this
place, in sufficient quantities for the manufacture of glass, or for sawing marble, should it ever
be required for such purposes. This kind of sand is found at intervals, and in great quantities
along the lake shore from the Irondequoit to Sandy creek. Magnetic iron sand and garnet
sand are also found in considerable quantities, and collected for writing sand. The iron is not
in sufficient abundance to be of importance as an iron ore. These two sands result from the
destruction of granitic rocks containing both iron and garnet.
Water and Springs.
All the water of the county, and indeed of the whole district, contains lime in some form,
being what is termed hard water. The county generally is well watered, though in some parts
water is not so readily obtained. Along the northern slope of the “Mountain ridge,” and
over the whole of the sandstone formation, water is abundant, either rising to the surface in
springs, or collecting in the low grounds and forming small streams. In digging wells, where
the sandstone approaches the surface, it is often necessary to penetrate the rock a few feet
before a constant supply of water is found. After ascending to the top of the limestone, wa-
ter is not so abundant. Few springs rise to the surface, and the water accumulating in the
low grounds and forming small streams, is dried up in summer, or lost in the fissures of
the rock; consequently, at such seasons the supply of water on the surface is very limited.
Water is obtained by digging, at different depths; sometimes at the surface of the limestone,
but commonly by penetrating it a few feet, and often to the depth of thirty or forty feet. In
these cases it is usual to find a cavity or fissure in the rock, which affords an abundant supply.
The water from the wells never overflows the surface, though from the dip of the rocks it
might probably be made to do so. The water all flows into wells from the north, as we would
MONROE COUNTY. - 427
expect from the dip of the strata; and in some cases a well dug to the south of one already
supplying water, will drain the latter entirely. In such cases, it is only necessary to excavate
the northern well deeper to obtain a supply. -
The southern part of the county is plentifully supplied with water, both from springs and
streams; though towards the northern limit of the gypseous marls it is often necessary to
penetrate these rocks to the depth of fifty to sixty feet, and in some instances to two hun-
dred and even three hundred feet, before a supply is obtained. The earthy or compact por-
tions of these rocks afford but little water, till penetrated to considerable depths; and when
it is obtained, it appears to flow from a cavity or reservoir in the rock.
Springs of hydro-sulphuretted water are of frequent occurrence in almost every part of the
county, but more particularly along that portion occupied by the shales, both above and below
the limestone. Some of these springs are celebrated, and are much resorted to by invalids and
fashionable visiters. Among these may be enumerated the Monroe springs, about five miles
from Rochester, pleasantly situated in a grove not far from the road leading from Rochester
to Pittsford. . - : ** - *.
There is a copious spring of this kind, rising to the surface, on the land of Timothy Colby,
in Ogden. There is also another similar spring, very highly impregnated with sulphuretted
hydrogen, in the northern part of this town. . .
The Riga mineral spring is said to be very beneficial in cutaneous diseases. This
spring rises from near the junction of the limestone with the gypseous rocks above. Inflam-
mable gas (carburetted hydrogen) rises from this spring in sufficient quantities to supply a
constant flame from a half inch tube. Iron is an ingredient of the water, as appears from
the tests applied, and the presence of some salt is indicated by its taste. The rock from
which the spring issues is a dark green gypseous marl. ^, - -
Many springs contain large quantities of carbonate of lime in solution, which, as the water
comes to the air, is deposited in the form of tufa, or a fine pulverulent marl. Where the
quantity is small, it forms the porous vesicular deposit called tufa ; but where the water is
abundant, or where the spring rises in a level tract or swamp, the deposit is marl. The most
copious spring of this kind is in Caledonia, Livingston county, though the deposit is chiefly
made in Monroe county. There is a similar spring at the source of Mill creek. After the
carbonate of lime is deposited, the water of these springs is nearly pure acid water.
Salt Springs.
There are several salt springs in the county, from which salt has formerly been made, but
they have been abandoned since the facilities of transportation have increased; and salt is now
obtained much cheaper from Salina than it can be made from these springs. None of them
appear to have been penetrated to a great depth, and in their present state are so much diluted
with fresh water that the saline taste is barely perceptible. Owing to this circumstance, and
to the impossibility of obtaining accurate local information, no estimate can be formed of their
value. All these springs appear to have their origin in the indurated marl of the Medina
- 54*
428 GEOLOGY OF THE FOURTH DISTRICT.
sandstone. Whether the decomposition of this marl affords chloride of sodium, I am not pre-
pared to decide; but we know that this mineral does result from the decomposition of the
shales above the sandstone. The shale along the Genesee below Rochester produces chloride
of sodium and sulphate of magnesia. - 3. -- -
The situation of the salt springs in Monroe county, is unfavorable to large accumulations
of water, and this may be the reason why they have not been more productive. Those which
I have observed are along the margin of small streams, and the salt water as it comes to the
surface is carried off by the fresh water, or becomes too much diluted.
Tufa, Marl, and materials for manures.
The substance usually denominated marl is a calcareous deposit from springs, but partially
decomposed calcareous shales are properly marls. - -
Rain water has the property of dissolving the calcareous rocks over which it flows, and
the water of many springs holds large quantities in solution. This property is owing to the
presence of carbonic acid gas in the water; when the gas is dissipated in the atmosphere, the
calcareous matter before held in solution is thrown down. The porous or more compact por-
tions of this deposit, usually containing incrusted plants, leaves and other substances, is called
travertine or tufa. Besides this, a portion of the deposit in some situations is of a fine pulve-
rulent texture, often containing great numbers of fluviatile shells. -
Wherever the calcareous rocks are exposed, the action of rain and the percolation of water
from the soil produce depositions of tufa. Along all the streams and rivers where calcareous
rocks form the banks, we find deposits of tufa collecting, and remaining attached to the rocky
cliff, till, from their increasing weight, they fall into the stream. . .
Along the Genesee river, below Rochester, are considerable accumulations of this sub-
stance. Vast quantities of calcareous matter are also carried down this river and smaller
streams, to be deposited in Lake Ontario, probably in much more extensive beds than those
found on land. - . . . . *
Tufa is mostly used for burning into lime, of which it affords a fine quality. The more
compact parts of it have been employed for building, and form a cheap and durable material.
When first removed from the ground, and while moist, it is easily cut or sawed, and is thus
shaped into blocks of any required dimensions. After exposure the moisture evaporates, and
it becomes very hard. - * * -
Deposits of shell marl are found in various places in Monroe county. The most important
locality is in the southern part of the county, along the course of Allen's creek in Wheatland.
The eastern part of this deposit extends southward into Livingston county. Tufa forms the
upper portion in many places to the depth of three or four feet, and below it is the shell marl
three or four feet thick. Some portions of the formation are nearly pure carbonate of lime,
containing abundance of the shells mentioned; in other places it is impure from admixture of
earthy matter. It extends in length about three miles, and in breadth from half a mile to one
MONROE COUNTY, - 429
mile. The general thickness is about five feet, though often much greater. At its smallest
dimensions, we shall find it 125,452,800 cubic feet, or 2,309,056 loads. -
Another extensive deposit of this material is found along the course of Mill creek, extend-
ing from its source to Cady pond, and filling the marshes around the pond for the extent of
many acres.” Its thickness is unknown, but in some places it exceeds three or four feet,
Tufa forms in many places, in exposed situations, along this deposit. The soil above these
deposits is usually a light, partially decomposed vegetable matter, allowing the water to pass
through it, by which means it soon becomes parched, and the crops perish. By spreading
on this soil a small quantity of clay or loam and the marl beneath, it could be made of the
finest quality. The partially decomposed vegetable matter is also one of the best manures
with marl or lime. - - .
In the town of Riga, on the land of Mr. Knowles, a deposit of this marl, of unknown
depth, covers thirty or forty acres. It has been penetrated ten or fifteen feet, without finding
its termination. The upper portions are very pure carbonate of lime, yielding lime of a very
superior quality. It is cut out, while moist, in masses of the form and size of bricks, and
laid in the kiln and burned. After penetrating this deposit about two feet, it becomes mixed
with sand and other impurities, rendering it unfit for lime, but not for manure. By accident,
several loads of this marl were deposited and remained for several years on a barren piece of
ground; afterwards this spot was ploughed, and has yielded large crops every year since,
though before it produced almost nothing. Strange as it may seem, this change in the charac-
ter of the soil was not attributed to the marl; consequently it has not been used on other parts
of the farm. Numerous other localities have been noticed, but these are the most important.
Those enumerated are upon the gypseous rocks, and similar deposits may be expected in the
low grounds throughout the whole of this formation, the extent of which may be learned by
referring to the Geological map. • , .
The decomposing gypseous rocks afford a marl, which is sometimes too clayey to be bene-
ficial as a manure, but in other cases it is valuable, especially when mixed with shell marl.
This marl approaches the surface in many places in the town of Pittsford, where it is of
a character well adapted for use on sandy lands. The same marl is seen east of Pittsford,
along the line of the canal, and at Fairport. Gypsum in small quantities has been found in
the marl at these localities. On the west side of the river we find the gypseous marl in Riga,
Chili and Wheatland, in some places approaching the surface, or appearing in the beds of
small streams. The only place where this marl has been applied is in the town of Wheatland.
Mr. Merry has used this and the shell marl, separately and mixed, and finds the results fully
to realize his most sanguine expectations. Used on the light vegetable soil of the swamps in
that neighborhood, this marl has produced astonishing results. A meadow of this kind,
which produced little or nothing, was dressed with this marl, and sown with timothy
* The source of this stream is a spring rising among the gypseous rocks. The spring in Caledonia, Livingston county, is the
source of the stream from which most of the marl of the first named locality is deposited. -
430 ...T- GEOLOGY OF THE FOURTH DISTRICT.
seed; and in less than ten weeks from the time of sowing, three tons of hay to the acre were
cut from the meadow. The composition of this marl is admirably adapted to fertilize such
soils, producing a mixture of calcareous, aluminous and vegetable matter. Without dwelling
on particular localities, we may observe, that this marl may be found on almost every farm
in the southern range of towns in this county. …”
Gypsum.—Plaster.
The gypseous rocks extend across the southern part of this county, occupying all that por-
tion south of Black creek, and between it and Allen's creek. In one or two localities gypsum
has been found south of Allen's creek, but the formation is soon succeeded by the corniferous
limestone. Plaster has been obtained in small quantities at Cartersville, in the town of Pitts-
ford, but the quantity was not sufficient for profitable working. At this place, the marl is
decomposed to the depth of fifteen feet, and presents the appearance of a greenish grey clay.
Marl of this character appears in several places along the canal, near this place and at Fair-
port, but the quantity of plaster contained in it is too small for working.
The workable beds of gypsum are almost wholly confined to the southern part of the forma-
tion. Along the valley of Allen's creek, and Mill creek, two miles farther north, most of the
plaster of Monroe county is obtained. Both these places are in the town of Wheatland. In
the towns of Riga and Chili, gypsum is found in thin seams, and small nodules disseminated
throughout the rock. In these place, marls, which readily crumble on exposure to the air,
can be substituted for gypsum. Until within a few years, the value of plaster, as a manure
or stimulant for vegetation, has not been generally appreciated, but it is now much used; the
demand is constantly increasing, and will doubtless continue to do so. It is mostly employed
on grass lands, particularly on clover, as preparatory to a crop of wheat. It is also used on
wheat crops in the fall and spring, and Indian corn is much benefitted by the use of plaster.
One bushel to the acre is generally considered a sufficient quantity for grass crops. ,'
The manner in which plaster affects vegetation, is asserted by Liebig to be by a decompo-
sition, in which the sulphuric acid becomes combined with ammonia, which then acts upon the
vegetation. This process, however, is not admitted by all to take place, and the operation of
plaster seems yet obscure. In the use of this, as well as many other manures, the fact is
overlooked, that plants are supported, in a great degree, by carbonic acid, and that much of
this food is taken up by that part of the plant above ground. In this view of the case, any
substance, above or beneath the surface, which presents carbonic acid to the plant, affords it
food. Thus many substances which do not enter into the composition of plants, afford much
food for them, either by absorbing this gas from other bodies and giving it to the plant, or
affording it from their own decomposition. . -
At present, about 5000 tons of plaster per annum are obtained from the town of Wheatland;
of this quantity, 4000 tons are used in Monroe county. This, however, is not the whole
amount used in the county, as much plaster is brought from counties further east. Of the
5000 tons, 1500 tons are obtained from Mr. Garbutt's farm, in the north part of Wheatland;
MONROE COUNTY. 431
1000 tons from Messrs. Sage and Harman's, the adjoining farm ; and 1000 tons from the
Messrs. McVean's farm, on lot 49. The remaining 1500 tons are supplied from an extensive
deposit at Garbutt's mills, on Allen's creek. Ground plaster is sold for three dollars per ton.
Metals.
Iron is the only ore of any importance in this county. Blende and galena (or the sulphurets
of lead and zinc) are found in the Niagara limestone, but never in large quantities. The
argillaceous iron ore, already noticed, extends from the Genesee river to the eastern limits of
the county, but has not yet been explored in any part of this distance.
Quicklime and Hydraulic Cement.
Quicklime is manufactured in considerable quantities from the Niagara limestone. There
are several kilns near Rochester, and others farther west and south. East of Rochester,
lime is made from boulders and fragments of limestone on the surface and imbedded in the
soil. This limestone contains magnesian earth, and some other impurities, rendering the
lime less valuable than it otherwise would be. In some localities certain strata only are used
for making lime, and in other places the whole of the rock is too impure for that purpose.
This is owing to the predominance of siliceous and aluminous matter.
Hydraulic Cement.
As this material is extensively used along the line of the Erie canal, it may be proper to
offer some remarks on the quality and situation of the substance used for this purpose.
Nearly all the hydraulic cement now used is brought from Onondaga.
I have already remarked, that there is no formation to which the term hydraulic limestone
is exclusively applicable. The upper part of the calcareous shale, as it graduates into the
Niagara limestone, becomes, by admixture of siliceous and argillaceous matter, a substance
considered fit for hydraulic cement. The upper portions of the gypseous rocks, by similar
admixture, become an argillaceous limestone, used for the same purpose.
From the circumstance that these rocks are an intermediate formation, or produced at
the passage of a shale into a limestone, no two strata are alike. For example, an upper
stratum may be nearly a pure limestone, while a lower one is almost wholly argillaceous;
thus no reliance can be placed upon its quality. The same stratum at different places may
also change the proportion of its component parts. The greatest objection in regard to the
stone used for this cement is, that it contains too much argillaceous matter, and for this reason
will never withstand the action of freezing water. Much of the cement now made is of very
inferior quality, and losses are constantly sustained from its use. This subject is one which
requires strict and constant investigation, and the State of New-York would save large sums
in the construction of her public works by procuring a cement of good quality.
432 GEOLOGY OF THE FOURTH DISTRICT.
The rock used in this county for cement, is usually blue or greenish blue, when first
exposed to the atmosphere, but becomes rusty grey and partially decomposed by atmospheric
agents. In the locality last mentioned, the original color of the stone is grey, or of the color
of pipe-clay. -" -
Fire Stone.
A stratum of light grey limestone, of a porous texture, extends through the towns of Ogden
and Sweden. This stone resists the action of ordinary fires for many years with little appa-
rent loss or change. Its character depends on the presence of magnesian earth, and the
porous structure of the stone, which prevents it from cracking when heated. It is much used
in this neighborhood for the backs and jambs of fire-places, and also for door and window
caps and sills. At the place where the stone is quarried, the stratum is not seen in place,
but masses of the broken outcropping edge are used. -
Some of the strata of the gypseous rocks are sufficiently siliceous to be a good fire stone,
and have been used for hearths of iron furnaces.
Materials }for Construction.
Common building stone is obtained in many places along the course of the Niagara
limestone formation. A very durable stone is quarried from the bed of the Genesee river at
Rochester, and has been used for the foundation of the new aqueduct. Some of the stone is
injured by the presence of thin seams of shale, admitting water, which, on freezing, will expand
and split the stone. The portions free from seams of this kind, furnish one of the best and
most durable materials in the county. A very good stone for ordinary purposes of construc-
tion is obtained at the rapids near Rochester; but owing to its geodal structure, it cannot be
used where a smooth and even surface is required. Dark, bituminous limestone is quarried
in several places in Penfield. - - - f
In West-Mendon the upper strata of the Onondaga salt group are extensively quarried for
step-stones, door and window caps and sills, lintels, blocks for corners, pedestals, etc. The rock
is a silico-argillaceous limestone, sufficiently hard and compact for ordinary purposes. When
first quarried it is soft and easily worked, but becomes harder on drying. This stone is much
used in Rochester and the adjoining towns, and the demand is constantly increasing. The
common thickness of the layers is from four to eight inches, and they can be procured of any
required dimensions. Except the more siliceous portions, these stones should not be used
where they will be subjected to the action of freezing water, farther than to rains, which seem
scarcely to affect them. - - - . . .
The Medina sandstone and the indurated marl of the same formation have been used for
building stone; but experience has proved what a knowledge of their composition would have
foretold, viz. that in Monroe county they are almost entirely unfit for any useful purpose
whatever. Many apparently compact blocks of this rock will, in the course of a few weeks,
if exposed, crumble into a loose mass. Where used in buildings, it has, in some cases, been
MONROE county. 433
little affected by the weather; but in most, it has been rapidly destroyed. The great objection
to the stone, is the presence of a large proportion of argillaceous matter, absorbing water,
which destroys it by the same process that the hydraulic cement is removed from the walls
of locks.
The limestone of Monroe county affords no marble or materials for decoration. The more
siliceous portions of the Niagara limestone furnish a fine material for macadamizing roads,
and it is much used near Rochester for that purpose. Paving stones are obtained from the
drift. Flagging stone is not abundant, but is found among the siliceous strata of the Onon-
daga salt group. * . -
The sandstone has been quarried near the outlet of Irondequoit creek, and used in the con-
struction of piers at the mouth of the Genesee river. By the action of the waves and freezing
water, it is very rapidly destroyed, and it becomes necessary to rebuild the piers almost
annually. The stone from this quarry has recently been rejected for the construction of
piers, and limestone substituted. An expense of several thousand dollars had been incurred
in opening the quarry, before the stone was rejected. Had the proprietors submitted it to
the examination of some competent person, or to the common tests, all this expense would
have been saved. - -
ORLEANS COUNTY.”
The rocks of this county consist of the same as those on the east, with the exception of
the Onondaga salt group, which has not been detected within its limits. The Niagara group
rises in a terrace above the surrounding country, becoming more elevated in a westerly direc-
tion. The Clinton group appears in much diminished thickness, but still highly fossiliferous.
The Medina sandstone abounds in fossils at Medina, that being the principal locality where
shells occur in this rock. The section from this place southward will give one a correct idea of
the strata. The vicinity of Albion and Farwell's mill, are also good localities for fossils in
the Niagara group. The Medina sandstone occupies more than half the width of this county.
Surface of the Country.
The most prominent character of Orleans, when compared with the adjoining counties, is a
remarkable evenness of surface. Indeed, the whole county, with the exception of its two
* The details of investigation in this county, are principally extracted trom the report of the late Dr. G. W. Boyd. (Annual
Report of 1838.) -
GEOL. 4th DIST. 55
434 GEOLogy of THE FOURTH DISTRICT.
ridges, may be considered as nearly a level; and in traversing it at any part in an east or west
direction, there is neither ascent nor descent of any consequence, nor any irregularity of the
surface, other than where the streams have worn down their present channels. This is espe-
cially the character of all that part of the country north of the Erie canal, from which to
Lake Ontario there is a gradual and almost imperceptible descent ; the country presenting an
uniform level face, with the exception of the ridge, on the summit of which passes the Ridge
road. The Erie canal is in this county at an elevation of 275 feet above the level of Lake
Ontario, and its distance from the lake is between eight and ten miles.
The level country continues south of the canal for about two miles, when we meet a sud-
den rise, upon ascending which, we arrive upon the limestone range. This rise bears the
name of Maple ridge at Shelby, two miles south of Medina; and following the course of the
canal, it is seen at Millsville; then going east it passes about two miles south of Albion,
preserving the same distance for two and a half miles, when it gradually inclines northward, and
crosses the Transit line at a road one and a quarter miles from the canal. Hence it continues
east, and soon reaches Jefferson lake, of which it forms the southern shore. From this small
lake it turns rapidly to the south, and reaches Clarendon centre; beyond which it continues still
south for about two miles, and then turning to the east again, passes into the county of Monroe.
This ridge, or terrace, has a pretty uniform elevation of about fifty feet.
From Maple ridge southwardly, the country has a very gentle rise for about two miles,
when we arrive at another distinct, but more moderate step, which is about thirty feet in height.
South of Shelby, this rise bears the name of Windfall ridge, and in other parts of the county
is known as Limestone ridge. Its course is east and west, parallel with Maple ridge, from
which it preserves a distance of about two miles, and can be followed from the western part
of the town of Shelby, passing by Barre centre eastward to the Transit line. After ascend-
ing this terrace we are on the summit of the limestone range, and on the highest ground in
the county. The country now continues quite level for about two miles to the south, and
then descends gradually to the Tonawanda marshes, which in this county are only ninety
feet above the level of the Erie canal. –
Lake Shore, Streams, etc.
The shore of Lake Ontario forms nearly an uniform straight line from east to west, and
presents a bank of moderate height, in general protected by a beach.
During the summers of 1836 and 1837, the lake encroached on the land. On the east side
of the Oak-orchard creek, three or four rods were removed, together with a fine beach of two
or three rods in width; so that at present the waves dash against and undermine the bank,
which is constantly falling into the lake. In the course of the summer of 1837, the bank,
for a limited extent, and to the width of 30 feet, was swept away by the waters of the lake.
At Torry's harbor, we noticed several small mounds, considered to be of Indian origin; and
similar ones are said to be numerous in the town of Shelby, a short distance south of the
canal. -
ORLEANS COUNTY. 435
Oak-Orchard Creek is the principal water course in Orleans county. On the east side of
the creek, at the mouth, we saw two or three mounds about three feet high, and ten feet in
diameter, containing human bones.
It will be noticed, upon reference to the map of this county, that all the creeks have a ge-
neral bearing to the east. This may be owing to the direction of the rock fissures, which are
generally northeast. - -
The Tonawanda marshes extend along the southern edge of Orleans county, and occupy a
part of Clarendon, Barre and Shelby.
Immediately south of the ridge, in the north part of Murray, is a tamarac swamp, about
three miles in length, which communicates at one end with Marsh creek, and at the other with
Sandy creek. Its reclamation has been commenced by drainage. -
Soils.
The prevailing character of the soil north of the ridge is sandy. Limited tracts of a clayey
nature occur, which were observed more especially near the lake. - -
Proceeding from Ridgeway to the lake, we find a sandy soil extending from the ridge to
within two miles of the lake; then clay predominates, and the soil consists of a clay loam,
which is a strong and warm soil, producing good crops. But little plaster is employed as
manure. - -- -
From Sandycreekville, the country inclines very gradually to the lake; about three miles
north of the village, we cross a tract of clay land about one mile in width. Two miles west
of the village, it approaches quite to the ridge. -
In Carlton, the soil is a sandy loam.
The northern part of Orleans embraces many fine farms, which although the soil is sandy, are
very productive. Farms immediately along the ridge are also more productive than we should
expect from the character of the soil; but the sand of the ridge we suppose to be not exclu-
sively siliceous, but to contain considerable lime. - - r
In the immediate vicinity of Albion, clay prevails in the soil; and about two miles east there
is a very sandy tract, of limited extent. - - -
The soil upon the limestone range in the towns of Shelby, Barre and Clarendon, appears to
be an excellent mixture of clay, sand and lime, and is very productive. But little plaster is
used in this part of the county, and there is evidently but slight necessity for it, inasmuch as
the soil is the result, chiefly, of the underlying limestones, and limestone shales. The road from
South-Barre to Clarendon runs upon the limestone range. -
55*
436 GEOLOGY OF THE FOURTH DISTRICT.
Springs and Mineral Waters.
North of the Erie canal, the springs and wells furnish good soft water. On the limestone
range, and in the county south of the canal, the water is hard, containing lime.
At South-Barre, limestone is found at the depth of seventeen feet, and water is generally
obtained at the surface of the rock, or upon penetrating it for a short distance.
The salt springs of Orleans county are in every instance upon the range of sandstone.
In the town of Ridgeway, one and a half miles north of Medina, near Oak-orchard creek,
is a saline spring, now neglected and nearly filled up, where salt was manufactured in the
early settlement of the county, more than twenty years ago.
A small salt spring is also known in the town of Gaines, at Fairhaven. -
In the town of Kendall, lot 137, now occupied by Mr. Hamblin, there is a brine spring,
at which salt was formerly made. -
Near Scofield's mills, Johnson's creek, in the town of Yates, salt was formerly manufac-
tured from a spring now neglected and filled up. -
A salt spring was discovered in the east bank of the Oak-orchard creek, at the village of
Oak-orchard, where salt was manufactured by Mr. Bennett. He bored to the depth of one
hundred and forty feet, and obtained a stronger brine, but the quantity was not increased.
The rock is red sandstone, of a soft, slaty nature. The works have been discontinued, and
gone to decay, and no taste of salt can at present be perceived in the water.
At Holley are three salt springs, formerly used for the manufacture of salt. They are all
situated in close proximity, in the bed of Sandy creek, immediately at the south side of the
culvert. One spring or well is now seen on the west side, and on a level with the bed of the
creek; having been neglected for some years, and having been exposed to overflow from the
creek, its proportion of saline matter could not be determined, but it has a decided brackish
taste. Another small spring is immediately opposite, on the east side of the creek; and here,
about four years since, borings were made to the depth of about thirty feet, but no subse-
quent operations were performed. A third spring was discovered immediately under the cul-
vert, and a wooden log was laid to conduct away the water. At present all these springs are
neglected. About the year 1821, considerable salt was made at these springs, and was sold
at five dollars per barrel; but when the Erie canal was constructed as far as Holley, salt
was brought from Salina, and furnished at a rate so low, that the works at this place and
others along the canal were at once discontinued. -
There are two sulphurous springs at Holley village, the water of which has been used as
a bath in cutaneous affections, .
ORLEANS COUNTY. 437
Clay.
Blue, yellow, and variegated clays, occur at many points in Orleans county, and are em-
ployed in the manufacture of bricks; as at Albion, where there are several kilns immediately
in the village. A fine blue clay was seen at Linden, a thriving village one mile south of
Yates centre. Blue and yellow clays appear at several points along the lake shore, forming
limited beds in the banks, but at present they are not explored.
Boulders.
A variety of primitive boulders were noticed along the Erie canal, between Hulberton and
Holley; also a little north of Medina, between the canal and ridge; and on the lake shore, in
Yates. In the northeast part of Barre, on the limestone range, one large boulder of granite
was observed, with greyish quartz and opalescent felspar. Also, at the same place, one very
large transported mass of sandstone.
These erratic blocks are found scattered over the surface, but I think in less profusion than
farther east. Near Jefferson lake are several large masses of granite, with dark blue felspar,
resembling the rock which occurs in place in Essex county, where it forms entire mountains.
At Oak-orchard, on the east bank of the creek, one small boulder was noted, consisting of
dark limestone, with fossils distinguished as belonging to the limestones which repose upon
the sandstone seen in the southern part of the county; but from its situation, it was considered
to have been brought down the stream by the high waters of the creek.
Marl.
There is a limited deposit of calcareous marl about one mile south of Holley, on the west
side of Sandy Creek. It is white, in a state of powder, and contains an abundance of shells,
principally the Helia albolabris (white-lipped snail). It occurs on the side of a hill, resting
on the red sandstone, and was exposed in digging a raceway.
Calcareous marl also occurs in a swamp on the farm of David Hooker, two and a half
miles north of Medina. - -.
Calcareous tufa forms in large quantities at the falls of Oak-orchard creek at Shelby, from
the decomposition of the calcareous shales.
Bog Iron Ore.
Several deposits of bog iron ore were noticed in the county, which, however, are not explored,
so that their extent is unknown. It occurs in solid masses one mile west of Albion.
One mile east of Ridgeway corners, on the south base of the ridge, bog iron is found in
grains, both loose and forming small masses in the soil, which is here a sandy loam. It has
438 GEOLOGY OF THE FOURTH DISTRICT.
the local name of shot ore. Bog iron also occurs one mile, and one and a half miles west of
Ridgeway corners.
In Ridgeway, between the ridge and west branch of Oak-orchard creek, there is a swamp
covering four hundred or five hundred acres, containing an abundance of bog ore, from which
iron has been manufactured.
Quicklime.
The limestone range in the southern part of this county furnishes an abundant supply of
materials for lime of an excellent quality. Kilns are erected south of Shelby, at Millsville,
about one mile south of Williams’s quarry in the town of Barre, and at other places in the lime-
stone region. At Barre, and on the range to Clarendon, the rock is of a light blue color, and
occurs in large irregular and ragged masses, either forming ledges, or scattered profusely over
the surface. It resembles very closely in character the limestone at the Bull's Head, one
mile from Rochester, and contains generally the same fossils.
Two miles west of Farwell’s mills, occurs a dark blue, bituminous, magnesian limestone,
containing fossils.
Hydraulic Lime.
We were informed that the upper layers of the rock at the falls of Oak-orchard creek, at
Shelby, are advantageously used for the manufacture of water cement. They consist of a
sandy limestone, but do not resemble in texture and other characters the best hydraulic lime-
stone. The cement used in the aqueduct at Medina was from this place, and has stood the
test of time as well as any other on the canal.
At Farwell's mills, Clarendon, there is a deposit of sandy limestone, slightly bituminous,
agreeing in texture, color and other characters, with the most approved hydraulic limestones
of the western counties, and, according to Judge Farwell, has been burned, and converted into
water cement of an excellent quality. This stone is also used for building.
Building and Flagging Stones.
The Medina sandstone prevails in the northern half of the county, and is exposed almost
continuously along the Erie canal, from Holley to Medina. North of the canal it is seen in
the banks or beds of the Creeks, and in other situations near the surface, which it immediately
underlies. It has been mentioned in the preceding pages, as frequently soft, argillaceous,
and not durable ; yet there are courses of this rock which are more dense, or siliceous, and
furnish an excellent material for building.
A little north and west of Medina is a quarry, which has furnished a handsome pink-colored
sandstone in large slabs and blocks, with Smooth surfaces and of good texture,
ORLEANS COUNTY. 439
The freestone was quarried on Otter creek, about two miles South of Eagle harbor, for some
of the works on the Erie canal. At this quarry the layers are thick, hard, not slaty, nor argil-
laceous as elsewhere, and yet it crumbles upon exposure. -.
In the southeast part of the village of Albion, a quarry was in operation, which furnished
rock of a reddish or variegated description, intended for buildings. The same quarry also
furnished courses of a grey sandstone of a firmer texture, with less argillaceous matter, and
altogether more durable. - - -
The upper layers of the sandstone near Albion consist of a greyish sandy rock, which is
preferred for the corner stones of buildings. The upper layers at Medina and Holley are
very siliceous, and too hard to be wrought with advantage. For foundations and rough work,
they are well adapted, and are of a texture to withstand the effects of moisture, frost, and all
other exposure. * .
The sandstone or freestone was also employed in the construction of the culvert over Sandy
creek at Holley; but the arch below showing a tendency to disintegration, a new one, com-
posed of limestone, was consequently built within, in order to sustain the first. We have
already mentioned that it was quarried near the mouth of Oak-orchard creek, and used in the
works pertaining to the harbor. -
The rock under consideratien is mostly inclined to disintegration upon exposure to the
weather, although quite firm when first quarried. In this respect it resembles the sandstone
of the Genesee river, below Rochester, of which it is a continuation. -
Thin layers of limestone are extracted from the bed of Oak-orchard creek, between Me-
dina and Shelby, and used at the former place for flagging. They appear to be of a siliceous
character, occur in large slabs, and the surfaces are frequently covered with fossil vegetables
of the family of fucoids; they strongly resemble the petrified stems of terrene plants.
Williams’s quarry, in the northeast part of the town of Barre, furnishes a siliceous or sandy
limestone, at present used for fences and underpinning, and which resembles the rock employ-
ed in Monroe county for the preparation of water cement. -
A grey, porous, siliceous limestone is quarried at Farwell’s mills, Clarendon centre, and
used in buildings. Some of the layers contain a considerable proportion of lime, although
they mostly consist of a porous, flinty rock, much resembling the French buhrstone. The
quarry is quite extensive, and occupies the summit of the ridge which overlooks the village.
Its porous structure is due to the removal of small fossils and fragments of crinoidal stems.
440 - GEOLOGY OF THE FOURTH DISTRICT.
i
§ º § N § # |
$$$. \\ § &. *"º
==S$ º \ºft
º . % % § º
ceº." º,
º
š
łº
gºal:HERRººmEBRITUTIIIHIELIHEſºgºniś - --
º -º-º-º: #; *::::::: º SS É ºn-lºs #
## - §§ |
- tºº
§ \
º § N § § s
\\ *] WW
\\ \\ \ t } \ .*
D a #º *::
B |
jº
YNº. |
&Fºix:
º #$$.
| Ż % B §§ |
%jš
º
tº: T
lº |
º
#
º ºurº
|
º j ſº
| %
\\ ill |# º [...] ºl -- £ E
.# #################
| -º-, L
|Hiſſillº §:
º
º .
†iº
HII: ºlº \
§º ſ
§
#. º
#ºft
#ºliń.
NIAGARA COUNTY.
We find the same rocks in this county as in the preceding ones. The Medina sandstone
forms a broad band on the northern side of the county, reaching nearly to the line of the Erie
canal, and the Onondaga salt group forms a narrow band on its southern edge. The Niagara
and Clinton groups form a high terrace, extending entirely across the county, and are only
interrupted at the Niagara river, pursuing their way beyond into Canada. This remarkable
terrace furnishes a good opportunity of examining the rocks of these groups, and no locality
offers so good facilities for this purpose as Lockport and the gorge of the Niagara.
Surface of the country — Streams, &c.
The Mountain ridge" is the most remarkable feature in the surface of this county. This
ridge gradually rises to the westward, and at the Niagara river is about three hundred and
fifty feet above the level of Lake Ontario, and two hundred and fifty feet above the country
on the north. At Lewiston, the whole descent to the north is made at one offset; but farther
east it descends by two, making two grand steps, or terraces. This double offset is produced
by the unequal hardness of the rocks; a stratum of sandstone causing the lower one, while
most of the rocks below and above it to the limestone are soft. In the eastern part of the
county, this stratum of sandstone has so far declined that it dips beneath the general level of
the country on the north. The mountain ridge passes through the towns of Lewiston, Cambria,
*—
“The terms “mountain ridge” and “terrace" have been used indiscriminately; the former is the name commonly applied, though
the latter is more appropriate.
NIAGARA COUNTY. 441
Lockport, and Royalton. From the foot of this terrace the country declines gradually towards
the lake, and the top of the terrace is the highest land in the county. From thence there is
a gradual slope south, to the Tonawanda creek. The streams flowing to the lake have cut
their channels deeply into the red marl and sandstone, and their great breadth and depth indi-
cate a much larger quantity of water at some previous time. -
The drift hills do not rise more than a few feet above the general surface. The soil every
where is composed, in part, of water-worn materials; but the hills, if there ever were any, have
been levelled by some subsequent cause.
In descending the terrace on the north, we find ridges of loose materials extending from
the top and sloping gradually off to the surface below. Where the northern extremities of the
hills have been excavated, we find large rounded masses of limestone and shale, from the
rocks south, with masses of granite. These are all mingled together in confusion; and the
masses of limestone are worn and scratched, as if having been borne along with blocks of
harder rock. From these appearances, and the form of the hills, it is very evident that a cur-
rent of water flowed from the south. But again, on the summit of this terrace we find masses
of sandstone from the north, often wedged into fissures of the limestone, as if driven there
by violent force. The following section of the cliff, and a superficial deposit of this kind, at
Lewiston, illustrates the subject. At the point a, which is just beyond the edge of the pro-
jecting mass of grey sandstone, there is an immense accumulation of partially worn fragments
of sandstone and limestone; large numbers of the latter being from the top of the terrace
above. This deposit has been penetrated seventy feet, without reaching the rock beneath.
192.
6 ºzºa
5 —ET--— - T-
**- *-----,
4. * * T -- ~.
- Z * = *— *{− .4-
£7, 6 2 ſ º, 2. ' . Af
1. - sºft ~~~~ * * * //
C ſº Tº: - - e * * …”
N ºšº *_w §§ & . ." . " . - → ~~~
£º šº ' ' , , , , , ~-
º .." f , f * , • / ge' Asº ~~~~ ºf
- -- Ar * *
1, 2, 3. Lower, middle and upper parts of the Medina sandstone. 5. Shale of the Niagara Group.
4. Clinton Group. 6. Limestone of the Niagara Group.
Several extensive marshes along the lake shore are gradually being filled with materials
brought into them by streams, and deposited, while the outlets are dammed up by beaches.
Swamps on the south side of the Ridge road contain deposits of partially decomposed vegeta-
ble matter, to the depth of three or four feet. When the swamps are filled with water, this
substance expands, and the surface is elevated considerably above the level which it occupies
when dry. When drained, and the vegetation burned, the vegetable soil below takes fire, and
is with difficulty extinguished. A swamp of this character commences five miles east of
Lewiston, extends three miles, and is about half a mile wide. The vegetable soil is from
[GEoL. 4th DIST.] 56
442 GEOLOGY OF THE FOURTH DISTRICT,
one to three feet thick, and underlaid by clay, though in some parts a deposit of calcareous
marl is interposed.
The vegetable soil of these swamps will eventually become peat; indeed its composition is
now the same, but it is not yet sufficiently decomposed to allow the particles to cohere. The
swamps south of the Ridge road can readily be drained, and will become fertile meadows.
The south part of Niagara county is not thickly inhabited: the ground is low and marshy; the
growth of timber, tamarack, elm, ash, etc. The land only requires draining to become as
good, or better, than any in the county. The junction of the limestone and gypseous rocks is
near the southern line of the county, and at this point we always find some of the best land.
The dam across the Tonawanda, near its mouth, is a serious impediment to draining this region;
and unless the streams flowing into this, are cleared from obstructions, and the accumulated
water carried off, the south part of this county and the north of Erie must long remain unim-
proved.
In following the lake ridge from the east to Eighteen-mile creek, it suddenly disappears,
and is again seen four miles farther west. When the lake was at this elevation, probably a
broad bay at the outlet of this creek prevented the continuation of the ridge. About seven
miles west of Eighteen-mile creek, the ridge divides; and a portion, precisely similar to the
continuous ridge, after extending two miles in a northwest direction, suddenly terminates.
This fork was evidently a bar projecting into the ancient lake.
Lake Shore.
The lake shore, forming the northern boundary of this county, rises abruptly to the height
of from ten to thirty feet. The bank is generally composed of gravel, sand, and clay, with
a beach of pebbles at its base. The lake at its present elevation washes the foot of the bank,
and in many places is undermining and wearing it away rapidly. On some farms ten feet in
width have been worn away in the course of a year, though the average loss of land may
not be more than four or five feet annually. Being upon the lake shore in this county
during a violent storm of two days (25th and 26th of October, 1837), I found that, during
that time, the soil to the width of three or four feet had been worn away. This effect was
not confined to a single spot, but extended for miles. The waves, during storms, are dashed
against the shore with such force that they are thrown entirely over the bank. It has thus
become a matter of much importance to the farmer, to protect his land against the ravages of
the lake. - - -
The Medina sandstone appears in the bank in many places, and at such points the land is
in a measure protected from the action of the waves. All the projecting points along the lake
shore are of sandstone, or marl of the same formation; and where it does not appear in the
bank, it is found at a little depth below the level of the lake. The most northerly point of
this rock on the lake shore is at least four hundred feet below the upper stratum of the forma-
t1On.
NIAGARA COUNTY. - - 443
The pebbles along the lake shore are red sandstone, and greenish blue siliceous limestone,
both containing fossils, the latter rock more abundantly. The fossils in these pebbles are
Corallines, Orthocera, bivalve and univalve shells. Both the character of the stone, and
the fossils, differ from any in the Fourth District. The mineralogical character of the pebbles
along the lake shore farther east, is very similar, but they contain no fossils. The pebbles
in the lake ridge, in Niagara county, exhibit the same fossils, and are precisely similar to
those on the lake shore, all being from the Hudson river group. -
Abraded materials from the banks are transported by the water, and form bars and shoals
at the mouths of smaller streams. The only river is the Niagara, and the immense body of
water brought down its channel entirely prevents any obstruction from depositions at its mouth,
though there is doubtless a vast deposit in the bed of the lake where the current becomes
neutralized.
Boulders.
Boulders of granite, and other rocks, are scattered over the northern part of the county,
in some places the surface being literally covered with them, while in the southern part they
are almost entirely absent. In this respect Niagara county differs from Monroe, where in the
southern part boulders are very abundant and of large size. They are more abundant in the
eastern part of this county than towards the Niagara river. These boulders appear to follow
certain courses, and to extend in great profusion over certain districts; this distribution appears
to have been governed by some law, and we may yet arrive at data which will enable us to
describe the drift, and its varying characters, with as much precision as we now do a stratum,
or a series of strata in an older formation.
Soil.
The soil between the mountain and the lake ridges contains a large proportion of clay,
although extremely fertile. The lake ridge and the soil, for a limited distance, on either side,
is sandy or gravelly. North of the Ridge road, the soil for a short distance is clayey, except
along the streams, where it is sandy. From the ridge to the lake shore, the prevailing
soil is sandy loam, of a yellowish color, inclining to brown where the sandstone approaches
the surface, as it does in many places. It contains carbonate of lime, which often cements
the gravel below the surface. All kinds of crops flourish on this soil; and wheat, in Niagara,
is considered better than in the counties adjoining. • -
The indurated marl, or marly sandstone, does not admit the passage of water; and when
it approaches the surface, unless on a declivity, the water is too long retained. The soil in
these cases becomes wet and cold, and in rainy seasons the crops are sometimes injured.
In some places in the northern part of this county there are alternations of a clayey with
a sandy soil, often several miles in extent; and generally, in this part of the county, the soil
seems divided into nearly equal proportions, in one of which sand predominates, and in the
other clay. The sandy portions are a little elevated above the loam or clay soil, as if trans-
56*
444 GEOLOGY OF THE FOURTH DISTRICT.
ported by a gentle current over the bottom of the ancient lake, which might move sand;
while clay, if once deposited, would be less easily disturbed.
The soil upon the mountain ridge is sand, or sandy loam, for a mile or two south, when
the proportion of clay increases. Along the Tonnewanda, clay soil predominates, owing to
the gypseous marls, which are argillaceous, in the lower part of the formation. These marls
extend into Niagara county, their outcrop being a little distance north of the Tonawanda creek.
Clays.
Beds of clay are found in every town in Niagara county, though many are of impure quality
from admixture of sand and carbonate of lime. The demand for bricks has, however, been
confined to one or two points, and consequently these beds have not been explored. The
prevalence of limestone, and limestone shale, more or less affects all the deposits of clay,
except those along the lake shore. *
Many of the bricks manufactured in the county are of inferior quality, arising from the
use of sandy loam mixed with the clay, instead of a pure siliceous sand. This loam contains
abundance of fine particles of limestone, and when burned, becomes lime: the action of water
on such bricks is rapidly destructive. - g
On the lake shore, a bed of clay continues almost from the eastern to the western extremity
of the county. In some places this thins out, and its place is occupied by gravel or loam, and
sometimes the clay is intermixed with one or both these substances; the upper part being
grey and less pure than the lower, which is usually of a bluish color throughout, or variega-
ted with spots of brown and green. Where the lower part of the stratum is seen, it rests on
a partially indurated deposit of gravel and clay, of a reddish color, and this rests upon the red
marl or sandstone. The clay is from two to six feet thick, and often contains pebbles and
boulders, similar to those on the lake shore. Frequently we observe alternations of the clay
and a part of the gravel stratum, below and above, and the clay is often much bent and con-
torted, although it rests on a nearly horizontal base. These alternations and contortions are
in many places very remarkable, and would induce the belief that almost any position, observed
in stratified rocks, may be given during their deposition. The presence of pebbles and boul-
ders in the clay, proves that the water from which it was deposited had sufficient velocity
to transport large and heavy materials. - -
The grey loamy clay above the blue clay sometimes attains the thickness of four or five
feet, and in some places the whole deposit is of this color. The grey, where it occurs, appears
entirely distinct from the blue, as if it might have been deposited at a subsequent period. In
this clay we find the calcareous concretions called clay stones, or “clay dogs,” which assume
all imaginary forms, sometimes the most fantastic. They are often spherical, and sometimes
two or more of them attached together. They appear at regular intervals in the strata, and
commonly a line of them marks the junction of the grey with the blue clay below, being at that
point where the surface water meets an impervious layer. These substances are an earthy
carbonate of lime, which is apparently deposited from the water precolating from the surface.
NIAGARA COUNTY. 445
Fibres (apparently vegetable) extend from the surface to the depth of three or four (sometimes
twelve) feet; and around these fibres, as a nucleus, the deposit is made. The grey loamy
clay is pervious to water, while the blue clay is not; and the fibres never extend into the blue
clay, but always terminate at its surface. We find the clay stones surrounding the same fibre
at different depths, and can often trace the connection of several; sometimes these are merely
rings of calcareous matter, the internal part still being clay. Those formed directly around
the fibre are usually perforated; but others are often attached on every side of this one, which
are entirely solid. It appears as if the water had been conducted downwards by this fibre,
and the solid material deposited, forming a ring. But when the accumulations are large, or
where the stratum below is impervious, the calcareous matter is forced out on every side, and
produces the fantastic forms which we so often find. - -
This deposit of clay is found on the Niagara river, and extending nearly a mile from its
mouth. At this place, the grey or yellowish clay above attains a much greater thickness than
at any other place. w - -
Sands.
No extensive deposits of siliceous sand occur in this county. In many places along the
lake shore, it appears in small quantities.
Water and Springs.
The county is well watered throughout, both by springs and streams. Along the foot of
the mountain ridge, numerous springs of fresh water gush out from fissures in the limestone,
or at the junction of the shale and limestone below. Water is readily obtained in almost any
situation, by penetrating a few feet below the surface. North of the mountain ridge, it is
sometimes necessary to penetrate a few feet into the marl or sandstone, before a sufficient
supply is obtained. - -
Springs of hydro-sulphuretted water,-‘‘sulphur springs,” are of frequent occurrence in
many parts of the county, but few of them have any celebrity. Some contain sulphate of
magnesia in solution, in sufficient quantities to affect the taste very sensibly.
Near Lewiston a copious spring rises from beneath the stratum of grey sandstone, about
one hundred feet from the top of the formation. The water of this spring is slightly
charged with sulphuretted hydrogen, and contains a notable proportion of sulphate of mag-
nesia. Its situation, however, is almost inaccessible, and for that reason will not soon become
a place of resort. Other similar springs, but less copious, occur in the vicinity. “ Sulphur
springs” are found in many places in the shale and limestone along the northern slope of the
mountain ridge. They occur wherever iron pyrites is disseminated through the rock. At
Lockport, in the limestone above the shale, a spring of this kind, when opened, discharged
gas sufficient to support a constant flame from a small tube. On the Tonawanda creek,
about two miles from the village, on the land of Mr. Vandenburgh, is a spring of this kind,
446 GEOLOGY OF THE FOURTH DISTRICT.
which has some celebrity. About three miles below Niagara falls, near the margin of the
river bank, there is a sulphur spring, which is prepared with accommodations for visitors.
I observed but one chalybeate spring in the county. This is on the farm of Capt. Leonard,
two miles north of Lewiston. There are several other springs at the same place, and the
water of some is said to yield salt on evaporation. Two miles east of Lewiston, a copious
sulphur spring rises from the shale on the mountain ridge.
Salt Springs.
In Niagara county, as in Monroe, we find salt springs along the course and in the beds of
almost all the streams in the northern part of the county. These springs are not copious, but
we frequently find three or four in the distance of half a mile. Several of these springs occur
along the course of Eighteen-mile creek, between Lockport and Lake Ontario. Salt springs,
affording small quantities of water, occur along Golden-hill creek and Johnson's creek. Salt
was formerly made from a spring within three miles of Lockport; which, at the time I
examined it, was filled with fresh water.
It is the general belief that the water of these springs increases in strength on descending
into the rock, but this may be doubted. At St. Catharine’s, U. C., a boring of five hundred
feet was made in the same rock, and it was found that the water at three hundred feet was
279 (hydrometer), and at four hundred and twenty-five feet, 299; but this degree of strength
was not constant at the same depth at different times. -
Tufa — Marl— Materials for Agriculture.
Tufa is found in small quantities in many places, particularly along the north slope of the
mountain ridge; but it nowhere occurs in such abundance as in Monroe county.
Shell marl is found in swamps between the mountain and the lake ridges. An extensive
deposit of this substance occurs in a swamp five miles east of Lockport: it has been used at
this place as a substitute for lime, but not as a manure. Several other swamps of a similar
character occur on the south side of the Ridge road. In the south part of the county, along
the Tonawanda creek, are found beds of marl, but the condition of the country will not
admit of accurate examinations. These beds being in low grounds, cannot be available till the
land is drained. . . . t
The lower part of the gypseous rocks extend into Niagara county, and where they approach
the surface, can be used to great advantage on Sandy soils. - -
The partially decomposed calcareous shales on the northern slope of the mountain ridge,
are a good material for manure on sandy lands; but the large proportion of argillaceous matter
precludes their use where there is already sufficient clay in the soil. -
NIAGARA COUNTY. 447
Metals.
Bog iron is the only metallic ore of any importance, and this is not found in sufficient
abundance for manufacturing. It occurs in beds a few inches thick in many places in the
northern part of the county, perhaps none more than six or eight inches thick. I collected
specimens from Lewiston, and Wilson. In both places the deposit covers a considerable ex-
tent of surface, but is of little depth. The rocks from which this ore is derived are shale
and sandstone, and the proportion of iron in these is so small that large deposits are not made.
The argillaceous iron ore of Wayne and Monroe counties is not anywhere found in
Niagara county, though the formation is continued. -
Blende (sulphuret of zinc) is found in cavities of the Niagara limestone at Lockport and at
Niagara falls, and sometimes disseminated in the rock. The quantity is only sufficient for
cabinet specimens. - x-
Quicklime and Hydraulic Cement.
The Niagara limestone is the only rock in Niagara county from which quicklime is made.
The lower portions only of this limestone, near its outcropping edge, are used for making
pure lime; any part of it, however, is pure enough for agricultural purposes.
It has already been stated that the outcropping edge of this limestone follows the course of
the mountain ridge, so that at a glance one may perceive in what part of the county lime is
manufactured. *-
Hydraulic cement has been manufactured from the impure limestone, forming the beds of
passage from the shale to the limestone of the Niagara group. In many places farther east,
the same bed in the mountain ridge furnishes the hydraulic cement used on the canal. That
furnished for the aqueduct at Medina was from this rock, which occurs at Shelby, two miles
south of Medina. The same strata extend across the county from near Middleport to Lewiston.
At many places along this distance a good cement may be obtained, but the best stone for
this purpose is near the top of the terrace at Lewiston. The stone at this place is a sili-
ceous limestone, with some argillaceous matter, and containing a small proportion of the oxide
of manganese. Owing to the presence of this ore, the stone presents a greenish hue when
first exposed, but finally becomes a rusty grey.
Materials for Construction.
Both the limestone and sandstone formations furnish good and durable materials for the con-
struction of buildings. There is a stratum of the sandstone formation about twenty-five feet
thick, which affords a very fine building stone; and from the peculiar smoothness of some of
the layers, it is often very beautiful. The stone is a very pure siliceous sandstone, separating
into laminae or layers of from one eighth of an inch to eight inches thick, with very even
448 (GEOLOGY OF THE FOURTH DISTRICT.
surfaces. The position of this stratum, or bed, has already been noticed as occurring in the
midst of the red marly sandstone. - •
The limestone, particularly in the lower strata, furnishes a superior stone for building. It is
only at intervals, however, that the same strata furnish a similar material; for at one point we
may obtain regular blocks of almost any required dimensions, and often at a short distance the
the same stratum is divided into thin laminæ. The best material of this kind in the county,
and indeed far the best I have seen in the district, is obtained at the Coldspring quarries
near Lockport. These quarries are at three points within a mile of each other, and within
three miles of Lockport. Two of the quarries belong to Mr. W. D. Shuler, and the other
to Messrs. Skinner and Day. Mr. Buell has since opened another quarry near the village of
Lockport. The stone is of a light grey color, generally compact, or sub-crystalline, though
often exhibiting a porous surface. They are among the most durable materials for construc-
tion, as may be proved by examining the locks of the canal at Lockport, where the same kind
of stone has been exposed to all changes of temperature, and to freezing water, and still remains
firm. Wherever this stone has been used in buildings, it remains unchanged by the action of
atmospheric agents. It is extensively used at Buffalo, Lockport, Rochester, and many of the
villages along the canal. The quarries are favorably situated, being on the brow of the
mountain ridge. .
Variegated Marble of Lockport.
At the village of Lockport, we find the same strata as at the Coldspring quarries; but here
they are more compact in texture, and contain abundance of fragments of crinoidal columns.
These columns, and a few other fossils in the rock, are of a reddish brown color, giving to the
surface a beautifully variegated appearance. The rock is sufficiently compact to be polished;
it has been used for some ornamental purposes, and is known as “Lockport marble.”
The variegated strata are from five to eight feet thick, and extend over an area of many
acres. This marble will doubtless become valuable at some future time, when the demand is
greater than at present.
Flagging Stones.
Flagging stones of the finest quality are obtained from the Medina sandstone. The princi-
pal quarry belonging to Mr. Whitmore, is one and a quarter miles northwest of Lockport. The
stone quarried for flagging occupies about five feet in thickness, of the upper part of the strata;
the stone separates into thin laminae or layers commonly of the thickness of two to four inches,
but often not more than the eighth of an inch. -
The slabs are frequently obtained twenty feet square, and no more than four inches thick.
One in the collection of the State, is six feet long, four feet wide, and little more than an inch
thick. From its even surface this stone is admirably adapted so the purposes for which it is
used, and the purely siliceous texture renders it extremely durable. It is now much used in
Buffalo, Lockport and Rochester.
SENECA COUNTY. 449
SENECA COUNTY.
All that part of the county north of the Seneca lake outlet, with the exception of a small
portion south of a line drawn from Waterloo in a northwest direction to Ontario county, is
occupied by the Onondaga salt group. Nearly all this northern part of the county is deeply
covered with alluvium ; and the rocks appear at very few points. One of these is in the bank
of Bear creek, where gypsum was quarried many years since; and another about three miles
north of Seneca-falls, where gypsum and gypseous marl were penetrated in digging a well.
The great depth at which gypsum is found in the north part of the county will, for the pre-
sent, and for a long time to come, preclude its profitable exploration. The waters of Seneca
lake, which have worn a recent outlet along the southern limit of this series, expose the gyp-
sum and associated rocks near Seneca-falls village, and for nearly three miles below. Along
this distance the gypsum is extensively quarried. It occurs in irregular, often conical masses,
enclosed in a greyish friable marl, with which it is often much intermixed, and in consequence
deteriorated in quality.
There is here no evidence that the masses of gypsum have forced up the strata, as noticed in
some places in Monroe and Ontario counties. On the other hand, the lines of stratification in
the marl are continued through the mass of gypsum without interruption. The strata are
undulated, the depressions being between the beds of gypsum ; and this appearance may
have been caused either from the porous nature of the marl by which some of it has been
dissolved and carried off, or from contraction, on drying of the mass between the gypsum
beds. The latter, being a chemical compound, and the force of aggregation greater on
becoming indurated, has contracted less than the surrounding marl; it consequently presents
a slight convexity in the surface. In these beds all appearances prove that the gypsum was
separated from the marl by chemical attraction, while each was in a fluid or semifluid state.
Small particles and seams of gypsum still remain scattered through the surrounding mass,
and it very appropriately receives the name of gypseous marl.
The rocks belonging to this formation are already described; they all bear much uniformity
in character at different points, and are easily recognized, even when the gypsum is not pre-
sent, by their argillaceous nature, and nearly uniform drab or ash color on exposure to
weather. Some portions are harder and darker, or frequently green on first exposure. Owing
to the usually soft nature of the strata, they have been removed from extensive tracts, and
the space filled with alluvium from more northern rocks; this is particularly the case in
Wayne, and the greater part of Monroe counties, as well as in Seneca and Ontario; and
from this fact, a principal member of the series, the red shale, has been overlooked.
Knowing the character of this rock, from examining other localities, we find evidence of its
existence along the northern part of this formation from the color of the soil; but after much
careful examination, I have not found a point between the Cayuga lake and Genesee river,
where that rock is exposed. Near King's corners, in the town of Butler, Wayne county, the
[GEoL. 4th DIST.] - 57
450 . GEOLOGY OF THE FOURTH DISTRICT.
soil for some distance along the road is of a deep red color, owing to the proximity of the
red shale: farther west the line of this rock is covered by deep alluvium, which in many
places is colored by the red shale. - -
The quarries below Seneca-falls are extensively wrought, and large quantities of the plaster
sent westward on the Erie canal, and southward up the Seneca lake, and thence by the Che-
mung canal; it is thus distributed over the counties of Chemung and Steuben. The quantity
of plaster annually taken from these beds is about five or six thousand tons. A small propor-
tion only of the vast quantity has been removed, and, at the present rate of consumption, it
will be long before these beds are exhausted. -,
That portion of the county south of the outlet and north of the turnpike leading to Cayuga
bridge, is probably underlaid by plaster, and the working of the beds on that side of the
outlet will gradually lead to its development. -
Above the gypsum, at this place, is a compact marl, containing small masses of granular
gypsum or selenite, which often appear to have crystallized in the fissures and seams. The
action of crystallization in this case appears to have taken place after the rock had become
partially indurated; and the indurated part of the marl in many places is filled with irregular
cavities, lined with crystalline carbonate of lime. This appearance may have occurred from
the rock having been broken up after partial induration, and thus forming with the gypsum,
then in solution, a kind of conglomerate, as is seen in some rocks below this. -
The soft gypseous marl, surrounding the beds of gypsum, could be very advantageously
employed on the sandy soils north of Seneca-falls, and west, towards Waterloo. The argil-
laceous matter of the marl would form with the sand a soil of proper consistence; while the
calcareous matter, and the small admixture of plaster, thus introduced, would be efficient in
promoting vegetation. -
On Black brook, three miles north of Seneca-falls, this mineral was obtained many years
since, but it has not been farther explored. At another point in the same neighborhood, a bed
was found in digging a well, thirty feet below the surface. This depth, however, will effect-
ually preclude any explorations for the mineral while it bears no higher prices than at present.
On the south side of the outlet, the beds probably continue an unlimited distance; but the
increasing depth of the superincumbent materials, from the dip in that direction, will effectually
preclude its exploration at this place. -
Along the south side of the Seneca outlet, the Corniferous limestone occupies a belt of
country about two or three miles wide, gradually approaching the stream about a mile west
of Waterloo village. • --
Along the area where this rock is exposed, there is evidence of several downheaves; pro-
bably caused by the solution and removal of the soft rocks below. These downheaves are
connected with, or produced by the same cause as those more important ones on the east side
of Cayuga lake, described by Mr. Vanuxem. No manifestation of disturbance appears on
the surface; the limestone is scarcely raised above the level of the surrounding country, and
the strata observed in the quarries all dip south at an angle of from four to six degrees
SENECA. COUNTY. 451
Noting the amount of dip in this rock, and finding it to occur frequently for a distance of
several miles, we might, at first view, be disposed to estimate it as of great thickness; but
in each of these quarries we find precisely the same rocks repeated, and the whole apparent
thickness consists of a few strata which have been several times broken up. -
In one of these faults, arises a copious spring of pure cold water, from the bed of which,
and over an area of twenty feet, nitrogen gas is abundantly emitted. No deposit of any kind
is left by the water, which through its whole course to the lake is remarkably clear and limpid.
The water from this spring, and another similar but much smaller one near, supplies the
Canoga flouring mills, a saw-mill and some other machinery. From no other spring in this
part of the State is nitrogen gas known to issue, all others known in the State being near the
junction of transition with primitive or metamorphic rocks. - -
The principal quarries of the Corniferous limestone are those of M*Allister, Rorison, and
one belonging to the county, adjoining the latter; half a mile south of the last is another
extensive quarry, and also one half a mile southwest of the Canoga spring. The stone is
quarried for buildings and enclosures, as well as for burning into lime. The layers do not
generally exceed a foot in thickness, and are separated by thin seams of shale. From six
to eight courses of the stone are to be seen in each quarry, which are generally separated
by thin seams of shale, and sometimes by a layer of hornstone; two or three of the latter
sometimes occur in the same quarry, separating the courses of limestone. The hornstone is
more commonly in courses of nodules in the limestone; sometimes one, and at other times
several courses, occurring in the same stratum of the different quarries. When dressed with
the chisel, it forms an elegant and durable material for stepstones, door and window caps and
sills. , " . - -
The Marcellus shale and the Hamilton group occupy a broad belt in this county. The
different members of the latter are well developed on the shores of both the Cayuga and Se-
neca lakes. These shales are chiefly interesting in the vast number of fossils which they
contain, and in the production of a calcareous soil. -*
Succeeding the Hamilton group we find the Tully limestone, the Genesee slate, and the
shales and flagstones of the Portage, group. -
Almost all the ravines where the Hamilton group is exposed, appear to have formerly been
large water courses, the present streams cutting a narrow channel in the bottom, which is
composed, sometimes to great depth, of water-worn fragments of shale and the rocks above,
and covered with soil supporting the largest forest trees. Along the banks of the ravines, the
destruction of the shale has produced a thin but rich soil, which, though the rains are constantly
washing it down into the valleys below, produces a small growth of trees, and a luxuriant one
of flowers, of which a greater variety and in greater beauty can scarcely be seen. The family
of Trillium, the C orydalis, Dentaria, Caulophyllum, Tiarella, and the delicate Mitella,
with hundreds of others, spring up in the greatest perfection and profusion. As beautiful
objects of natural scenery, these ravines cannot be surpassed. - -
Localities of the shale of this group are so numerous that it is unnecessary to enumerate
them all. The shore of Seneca lake, from three miles above the outlet to Goff's point, pre-
57%
452 GEOLOGY OF THE FOURTH DISTICT.
sents an almost continuous exposure of greater or less height. The western shore of Cayuga
lake, and for nearly the same distance, exhibits these shales, but not in high cliffs as on the
other side of the county. . - -
The Tully limestone is one of the most important rocks of the county, furnishing a supply
of lime along its line of outcrop, from ten to twelve miles south of the Corniferous limestone.
There are a few localities where this rock is very compact; the layers are from one to two
feet thick, and it can be quarried of any required dimensions. Its northern edge extends in
a curve entirely across the county. From where it is first seen, it may be followed in a north-
easterly direction to a point two miles north of Ovid village, where it is quarried for burning
into lime, and for various other purposes, on the land of Mr. Thompson Johnson. This point
is the greatest northern extension of the curve. From here it gradually bends to the southeast,
and appears on the Cayuga lake shore, in a line nearly east from its point of appearance on
the shore of Seneca lake. This curved outcropping of the massis merely the effect of erosion;
the greatest force of the northern current being in the channels of the two lakes, its power was
diminished towards the centre of the county, which consequently left the limestone extending
farther north at this point. - -
The Genesee slate, resembling very nearly in appearance the black shale of the coal for
mation, has been mistaken for the same ; and explorations for coal have frequently been
undertaken at great expense, resulting in final disappointment and loss. Most of the excava-
tions for coal in this part of the State are made in this shale, or the next succeeding group,
which often contains fragments of vegetables. The emission of inflammable gas, particularly
when arising from this rock, is supposed to proceed from beds of bituminous coal. Although
the fallacy of such a supposition has been frequently shown, the opinion is still entertained.
In the rocks of the Portage group, in this county, we find large numbers of fragments of
what appear to be terrestrial vegetables; some of these are several feet long, producing a
seam of coal of the same dimensions. These appearances have been sufficient to induce a
belief in the existence of workable beds of coal, but I need not say that such a Supposition is
entirely unfounded. -- - .
About four miles south of Lodi village, an excavation for coal has been made in the rocks
of this group. The principal inducement in this case appears to have been iron pyrites and
the sulphurous odor of the water, which is covered with a film so common in water flowing
through pyritous or other rocks. Petroleum also occurred in globules on the lower surfaces
of the slaty layers, which circumstance was considered by an “old miner,” who directed the
excavation, as a sure indication of coal. When I saw the place, the original excavation was
filled with dirty water, and the shales thrown out were nearly dissolved into soil. - .
Some good flag-stones are obtained from this group in the town of Lodi, and there are nu-
merous localities where these may be obtained in this part of the county.
This group is exposed in many of the ravines south of Lodi village, on the Seneca lake
shore; also in the same latitude on the Cayuga shore, in the south part of Covert, and in the
ravines extending towards the middle of the county. .
ONTARIO COUNTY. - 453
The principal building materials are the Corniferous limestone in the north, and the thin-
bedded sandstone in the south part of the county. - -
Calcareous tufa and marl occur in small quantities in several places; but from the nar-
rowness of the county, descending on either side to the lake shores, there are few situations
admitting of large accumulations. The most extensive which I have seen, is on the farm of
Mr. Dunlap, near the village of Ovid. - - . .
This county possesses few mineral resources except gypsum, being eminently agricultural
with a highly fertile soil. The northwestern portion is somewhat sandy, becoming loamy on
the south side of the outlet, while some portions east of this are quite clayey. The prevail-
.ing soil of the higher parts of the county is a clayey gravel. . -
Northern boulders are rare in this county, though the rocks of the northern part of the
district are largely intermixed in the soil. -
-QNTARIO COUNTY.
In this county we find the same rocks, and in the same general order, as in Seneca. The
“Saliferous Group of Onondaga " occupies that part of the county which lies north of a line
drawn from a point one mile north of Oak's corners, in the town of Phelps, along the course
of the Canandaigua outlet to Manchester, and thence west to Victor. The vast accumulation
of drift, however, leaves the rocks exposed but at few points, which are mostly along streams.
In a few cases, what appear externally to be drift hills are isolated masses of gypseous marl,
etc. deeply covered; and in some instances small masses of gypsum have been found in these,
much above the ordinary level of the valleys and surrounding country. Admitting that the
gypseous rocks originally held a higher elevation, and equal to that of the drift hills, before
the intermediate portions were transported southward, the fact proves the vast quantity of
matter removed by this agency. . . -
This group of rocks is much better exhibited in Ontario than in Seneca county, having a
greater extent, and in one or two places developing a different character. The gypsum here
occupies three distinct ranges; the northern or lowest appearing upon, or just north of the
county line, and the other two within the county. In the first the gypsum is associated with
a grey marl, which reposes on a green marl containing no gypsum. The grey marl exhibits
iron stains and decomposing pyrites; and pyrites is also found with the plaster which occurs
in small irregular masses, having a granular or crystalline texture, and frequently accompanied
by selenite. Masses of selenite are very abundant in the marl, varying from the size of a
walnut to several pounds weight, isolated as regards themselves, and having no connection
whatever with the larger masses of gypsum. In appearance and mode of formation they are
very analogous to those found in the Tertiary clays. The limpid selenite often embraces a small
454 GEOLOGY OF THE FOURTH DISTRICT.
piece of solid marl, having its faces and edges grooved or striated as in the pseudomorphic
crystals of common salt. The grey marl is also traversed by seams of gypsum, generally
flesh-colored or reddish, in such quantities that the whole is ground and sold for plaster. Both
the green and grey marl rapidly disintegrate, and form a tough clayey soil. -
The second series is developed near Port Gibson, and also about a mile distant, at an ele-
vation of twenty-five or thirty feet above the Erie canal. An argillaceous limestone appears
on or near the surface in low knolls or hillocks; this rock, on removal, is found to be frac-
tured, as if upraised from beneath, and at the depth of four or six feet, is found a flattened,
spheroidal mass of gypsum, quite disconnected with the surrounding rock. This gypsum is
fine-grained, compact, contains no selenite, and in general appearance is quite different from
that last described. The surrounding fractured rock is in thin layers from four to six inches
thick, which break into pieces from one to three feet square. The surfaces present numerous
little seams or cracks, similar to those produced in clay on drying; and the sides of these are
all smooth, and appear worn as if by the passage of water.
This character is very constant, so far as has been observed, and serves better than any
other to distinguish the rock. The external color, after weathering, is that of common clay;
on fresh fracture it is bluish, often nearly black. Water is with difficulty obtained along the
extent of this formation; the fractured rock beneath admitting the percolation of water so
rapidly as entirely to drain the soil, the little hillocks become in summer too dry to support
vegetation. Very little gypsum has been obtained from this series in Ontario county, though
it seems to be the same which furishes a great part of that mineral in Monroe county. It
will doubtless be explored, after the supply along the Canandaigua outlet in Phelps becomes
exhausted. -
The third series embraces the gypsum which is extensively quarried in the town of Phelps,
between Vienna and the town line of Manchester, along the Canandaigua outlet. West of
this point, one or two masses are seen in the bank of the outlet; and with this exception, and
a single bed recently opened near Victor; the town of Phelps furnishes all the gypsum from
the county. This, with its associated rocks, are very similar in character to those on the
Seneca outlet. It occurs in the same irregularly shaped or somewhat conical masses, pro-
ducing no disturbance in the surrounding strata, while the lines of stratification in the marl
pass through the beds of gypsum, and in several instances where one or two thin courses of
hard argillaceous limestone occur in the former, these also are continued through the latter,
the intervention of the rock merely breaking the continuity of the plaster, without otherwise
affecting it. In this series, the force of aggregation or chemical attraction seems not to have
been sufficiently powerful to separate the gypsum from all surrounding materials, consequent-
ly we find it much intermixed with the marl; and wherever the attraction of particles was
stronger than in either of these, as in the limestone, the strata continued their course through
the mass, scarcely interrupted at all. The greater tenacity of the latter may have prevented
the mobility necessary to an entire separation of particles, and from this cause in part may
arise the admixture of substances. -
ONTARIO COUNTY. - 455
The course of the Canandaigua outlet, from Manchester village to near Vienna, is along
the line of the Saliferous group and Water-lime, leaving the latter entirely on the south, and
the former, with the exception of a few beds, on the north. East of Vienna, all the marl and .
gypsum has been removed, and is replaced by a deep deposit of sandy alluvium. In the west
of Manchester, the same thickness is observed; and on the north side of the outlet, instead
of the gypsum, we find alluvial hills rising eighty or one hundred feet above the valley, but
not appearing south of the stream. From Manchester to the west line of the county, a low
valley extends along the southern boundary of the gypseous rocks, with alluvial hills rising
on its northern side. The original course of the Canandaigua outlet appears to have been
north; and it is very evident from the character of the rocks along which it passes, after
turning east, that this portion at least was excavated recently, or long after the deposition of
the alluvium, which may have closed its northerntegress. w
The principal quarries of gypsum are those of Robinson, Norton & Co., Cook, Vander-
mark & Co., and Hildreth. From these about six thousand tons annually are ground at the
mills on the outlet, and sold within the county. The-supply is sufficient for a much greater
amount, and unless the demand increases, the quarries will not be exhausted in many years.
Whenever this happens, explorations will extend north of the present quarries; and in all the
valleys along the north part of the county, the middle series of plaster beds will probably be
found. - -
The water-limes are better developed in this county than in Seneca, appearing in their
characteristic drab color. The mass may be traced almost uninterruptedly from near Oak’s
corners, in Phelps, to Manchester village; and beyond this it appears at many points, as on
Mud creek, and near Victor village. East of Vienna, all the strata of this division are highly
calcareous, and burned only for common quicklime. The principal quarries and kilns are
within one and a half miles of the village. It is also quarried for buildings and enclosures,
the layers being sufficiently thick. It becomes stained with iron on exposure, and in almost
every locality it is highly bituminous. -
At West-Vienna, this rock is burned for hydraulic cement, and is said to produce a very
good quality. Two miles farther west, at the quarry of Mr. Maffit, large quantities have been
used for this purpose. At this place, the stone varies little in external characters from that
used for lime. It consists of three distinct varieties: two only are used for the cement, while
the lower course is composed of thin layers of tough argillaceous, bluish limestone, breaking
on exposure into small irregular fragments; and in mineral character, it is precisely the same
as the strata which, pass-through the gypsum beds on the north side of the Canandaigua out-
let. This portion, on burning, melts into a coarse porous slag, externally glazed and yellowish.
The second stratum consists of thin layers, externally drab-colored, siliceous in texture, and
harsh to the touch. This is succeeded by a few layers of irregular thickness, lighter in color
than those below, and much more calcareous. Of the two last mentioned, each at intervals
partly takes the place of the other, so that their thickness is variable, and the dividing line
takes an undulatory direction. The whole depth of the two masses together varies from
three to seven feet. If the lower of these is burned alone, the cement will not “set” under
456 - GEOLOGY OF THE FOURTH DISTRICT.
-*
water; and if the upper is burned alone, it is found to be too calcareous, and less enduring
than the more siliceous cements. To obviate this difficulty, both are burned together, but
without regard to proportions. From the nature of the materials, it is evident that the pro-
portions of siliceous, argillaceous and calcareous matter must be very variable; and too little
attention has heretofore been given to this circumstance, and to the nature of the ingredients,
in the manufacture of hydraulic cement. *
West of the last named quarries, the water-lime appears in numerous localities south of
the outlet, and near the road leading from Vienna to Manchester; but here it is used mostly
for enclosures, and at Manchester village for building stone, some of the layers being two or
three feet thick. It is too soft and argillaceous for hydraulic cement or good lime. Above
the village of Fredon, this rock is exposed in all its varieties, for half a mile on Mud creek ;
and along the whole line from Manchester to that village it approaches the surface, and could
easily be obtained in any required quantity. Thence it extends west to the quarries in Men-
don, though the surface of the intervening space is mostly covered with deep alluvium.
The Oriskany sandstone appears in this county, upon Flint creek, at Vienna; it is not
seen in Seneca county, though loose fragments containing the characteristic fossils are scat-
tered upon the surface. At the locality just named it is a coarse porous sandstone, destitute of
fossils, so far as observed, with the exception of a single specimen of Ichthyodorulite; the large
Atrypa and Delthyris, which characterize this rock farther east, being entirely wanting. Its
purely siliceous character and porous texture are well adapted to withstand the effects of rapid
heating and cooling; it is much quarried for firestone, and used in the Ontario furnace, and
in the glass furnace at Clyde. It contains numerous small geodes lined with chalcedony;
also rounded masses of a dark rock are imbedded in its surface. These, on examination,
prove to be very compact aggregations of fine sand, colored with carbonaceous matter, and
may have resulted, as well as the chalcedony, from the long continued action of thermal
waters. - . - -
At the place where this rock is quarried, it is four feet thick, divided into two or three
layers, one of which is about two feet. It rests immediately on a slaty, argillaceous lime-
stone, four feet thick, which succeeds the water-lime proper. -
The Onondaga limestone, which, when free from seams, is perhaps the most durable of
the limestones, and one of the most beautiful for buildings, is much quarried at Oak's corners,
its eastern limit in Ontario county. - -
West of Vienna this limestone spreads out over a great surface, covered only with a thin
coating of soil, and having its northern termination about a quarter of a mile south of the
Canandaigua outlet. The principal quarries in this neighborhood are within two miles of
Vienna, these have furnished materials for locks on the canal, for building and step-stones;
and some partially crystalline portions, from the unequal expansion, form a good firestone for
the ordinary heat of a fire-place. At these quarries four layers of limestone are exposed,
two of which only are workable, the others being too thin, or separated by seams. The upper
one has in many places been nearly destroyed by the action of running water. -
The Corniferous limestone succeeds the Onondaga, and in some instances alternates with
ONTARIO COUNTY. 457
it. In Ontario county it follows the same course, and can be seen a little south of its out-
cropping edge. It is recognized by its darker blue color, fine texture and homogeneous struc-
ture; it is generally very brittle, breaking with a slight blow of the hammer, while in some
localities it furnishes stone fit for building. -
The Marcellus shale, and the shales of the Hamilton group, appear at numerous points in
this county; and after leaving Geneva, they may be seen in nearly all the ravines and banks
of streams which flow towards the north. The banks of Canandaigua lake also afford good
opportunity of examining these rocks. In other parts of the county, the accumulation of
drift is so great as to offer few exposures of these shales. - - r
The Tully limestone appears on the shore of Seneca lake, at Bellona, in the bed of Flint
creek at Bethel, and about four miles northwest of this point. Before reaching Canandaigua
lake, however, this rock has entirely thinned out, though its place in the shales is well defined
for many miles along the shore. - .
South of the range indicated by this limestone, there is a width of from one to three miles
of the Genesee slate, but this rock is only seen along the ravines. The gas springs of Bristol
and other places rise from this shale, or the lower part of the group next succeeding it.
The Portage group occupies the towns of Naples, Canadice, and the south part of Bristol,
and presents the same essential characters as described in Seneca county. The sandstone
portions are used for flagging stones, and, when sufficiently thick, for building stones.
These rocks are seen to great advantage in the deep ravines about the head of Canandaigua
lake, and in the banks of the Honeoye, Canadice and Hemlock lakes. These three lakes at
present join their outlets, producing the Honeoye creek, which has been excavated since the
deposition of the drift; and the rocks are exposed along its whole course. The original
outlet of these valleys was probably farther east, and joining the present Irondequoit, passed
into Lake Ontario by that channel. These valleys also extend south, and meet the Conhoc-
ton, showing that at some former period the course of the water was not restricted within its
present limits, but extended south to the Tioga or Chemung. Thus a stream whose width
embraces the valleys and beds of the lakes in this direction, may have passed southward from
Lake Ontario to the Susquehannah; or, otherwise, a stream from the south may have flowed
along the Conhocton and these valleys to Lake Ontario. It is quite evident, from the extent
of the valleys and the alluvium piled up in their course, that few of our streams in an earlier
geological era had their present origin, or were limited to their present extent. Every valley
and every rock bears marks of the great body of water of which small under currents merely
wore the course of the present valleys, while the mighty whole passed over the summits of
our highest hills. . - -
The principal mineral resource of this county is gypsum, the situation of which has already
been described. There are several marl beds of importance; the most extensive one is in a
marsh bordering Flint creek, south of the village of Bethel. Large quantities could readily
be obtained at this place, and it would prove a valuable acquisition to the farmer, especially
[GEOL. 4th DIST.] - 58
458 GEOLOGY OF THE FOURTH DISTRICT.
when combined with the muck with which it is deeply covered. There are several small de-
posits of marl near the northern edge of the county, upon the Onondaga salt group. There
is a large muck swamp near Victor, which is probably underlaid by marl. This substance
will, without doubt, also be found in the swamps at the head of Hemlock and Canadice lakes.
YATES COUNTY.
The rocks occupying the greater part of Yates county are similar to those of the southern
part of Ontario, only the most elevated parts of Barrington and Starkey being occupied by the
rocks of the Chemung group. The outlet of Crooked lake has excavated its channel through
the rocks of the Portage group, Genesee slate, Tully limestone, and the upper part of the
Hamilton group, presenting all these in their order along its course.
Northwestedly from Penn-Yan, and at Shepherd's quarry, the rocks of the Portage group
are well developed. At this place the lower part consists of alternating arenaceous and argil-
laceous strata, containing much iron pyrites, large fragments of carbonized vegetables, and
occasionally large Orthocerae. - - - -
The lower part of the group furnishes large and fine flag-stones, which are used in the streets
of Penn-Yan. These thin layers often contain small irregular concretions, surrounded by a
coating of shale which soon disintegrates, and the concretions become loosened, in many in-
stances injuring the stone. Some of these strata are shaly, and soon wear away on exposure.
This group appears about a mile south of Penn-Yan, in Sartwell's ravine, where its con-
nection with the black shale below is very evident; the characteristic Lingula of the latter
is found in abundance. - . -
The same group extends west through the towns of Jerusalem and Italy, and appears in
many of the streams and ravines near the west branch of Crooked lake. The thin layers of
sandstone are used throughout the country for step-stones, foot-walks, and in many instances
for enclosures, though rarely for building stones.
The outlet of Crooked lake affords a good opportunity of examining the higher part of the
Hamilton group, and its connexion with the Tully limestone and the higher rocks.
The lower part of the Portage group is developed near Penn-Yan, and on the west bank of
Crooked lake ; it presents a more arenaceous character than on the Genesee river, and contains
some fossils not seen elsewhere. -
From the nature of the strata, there are few economical mineral products in this county. The
outcropping of the Tully limestone along the Crooked lake outlet, is of great importance in
furnishing lime. Farther south, near Big-stream point, where this rock is concretionary in
structure, it affords a good hydraulic cement, which promises to be of importance to this
part of the county.
YATES COUNTY. - 459
Calcareous tufa occurs in several places along the banks of Crooked lake outlet, and marl
may be found in the swamps at the northern extremities of the lake. -
Under the head of Salt springs, has been noticed the occurrence of saline matter in the
springs about the head of Seneca lake; a similar spring was found near Big-stream point.
IBetween Seneca lake and the east branch of Crooked lake, a high ridge or elevated plain
slopes gradually to both, being divided transversely by the ravines and streams. Another ele-
vated table land, varied by slight undulations, rises between Seneca lake and the valley of Flint
creek, which extends to the head of the west branch of Crooked lake; this is interrupted by a
depression to the northeast of Penn-Yan. Another similar portion, though more irregular,
rises between the valleys of Flint creek and Canandaigua lake ; and the part of the county
between the two branches of Crooked lake terminates in a high bluff, called Bluff point.” From
near the head of the west branch, extending quite across the peninsula, is a valley which ap-
pears once to have connected the two branches, the highest point of which is not now more
than one hundred feet above the lake. * . --- -
LIVINGSTON COUNTY,
The county of Livingston exhibits a continuation of the rocks of Ontario, beginning with the
Water-lime or upper part of the Onondaga salt group, followed by the Onondaga and Corni-
ferous limestone, the Marcellus shale, Hamilton group, Genesee slate and Portage group;
the latter occupying the high grounds in the southern part of the county. - -
The deep depression of the Genesee valley, which extends through the centre of the county,
from south to north, is among the most important features of the county. - -
The thick-bedded hydraulic limestone in the northern part of the county, passes through
Caledonia and Avon. In the former place it is quarried in several localities. It underlies the
village of Caledonia, extending thence southeasterly toward the Genesee river, reappearing
on the other side, and extending northeasterly to Mendon. This rock is chiefly quarried for
buildings and enclosures. In several instances where it has been burned for cement, it has
been found unfit for the purpose, either from improper composition or from the mode of
burning. - . . - - -
* This point is said to be the locality of native iron, an account of which appeared in the Transactions of the Geological Society
of Pennsylvania, Vol. I. page 358; and since it has been quoted elsewhere, I may here give the true explanation. The rocks of
Bluff point are of the Portage group, which often contain iron pyrites. In quarrying stone at this place, a considerable quantity of
this ore was found; and as it was supposed to be valuable, it was shown to Dr. Sartwell of Penn-Yan, and afterwards to Prof.
Cutbush of Geneva, both of whom inſormed the persons of its true nature. Not feeling satisfied with this, however, it was
placed in a blacksmith's forge, and by much labor partially reduced ; and in this state a portion of the mass was sent to Mr
CŞemsen of Philadelphia. &
58*
460 GEOLOGY OF THE FOURTH DISTRICT.
For a distance of two or three miles southeast of the village of Caledonia, thin flat masses
of the drab limestone are scattered over the surface, in many places in sufficient quantities for
enclosures; its outcropping edges often approach so near the surface as to be turned up by
the plough. Three and a half miles southeast of Caledonia, it is quarried in large quantities
for use on the Genesee valley canal. The quarry is owned by Mr. Wadsworth of Geneseo.
There are about twenty feet in thickness of the rock exposed; the lower part is in thin layers
of a bluish color, striped with lighter bands. The succeeding courses are from two to two
and a half feet thick, of a drab color, striped with darker. It is easily quarried, splitting into
masses of any dimensions, and becomes very hard and brittle on exposure. The upper seven
feet of the mass is often in one course, though generally divided into two; this portion, and
a course of two feet below, contain numerous irregular cavities, often filled with greenish
clay, gypsum, sulphate of strontian, blende, etc. In some of these cavities there are remains
of some coralline fossils, the greater part having been dissolved out, probably by the action
of sulphuric acid, which formed, with the lime, gypsum, and with strontian its sulphate.
The same causes which here produced the small nodules of gypsum, were in operation
over a large extent, to form the immense quantity which occupies a place in the rocks beneath
the drab limestone. Owing to this circumstance only, we find no fossils in the gypseous rocks;
for none could exist in a sea where sulphuric acid was a free ingredient. -
The Onondaga limestone is but a thin mass in this county, scarcely appearing except in a
few localities. The principal of these is at Caledonia, and extending for several miles north-
west from the village. It abounds in its usual coralline fossils, but there are no places where
it is sufficiently developed for quarrying. .
The Corniferous limestone succeeds the last described rock; it scarcely extends into the
town of Lima, but forms the substratum of the northern portion of Avon, and in the river
valley extends as far south as the centre of the town. This rock is quarried in the Conesus
lake outlet, and on a small stream a short distance further east; at these places, only a few
feet of the upper part of the mass are seen. It is easily quarried in blocks of large dimensions,
and is nearly free from hornstone. The stone is wrought for use on the Genesee valley
canal. The fossils at this place consist chiefly of Strophomena rugosa, Atrypa affinis, Del-
thyris, and some fragments of trilobites. The greater portion of this rock, on the east side
of the river, is covered by a deep alluvium, which renders it difficult to trace its bearing and
outcrop with extreme accuracy. -
On the west side of the river, this rock first makes its appearance in the southeast corner
of Caledonia, near the town line. At this place a very extensive quarry has been opened, on
the west bank of a small stream, on land of Mr. Christie. Large quantities of stone have
been taken hence for the construction of locks, aqueducts, etc., for which purpose no
better stone can be found. It is mostly free from seams, and is easily quarried and dressed.
The whole thickness exposed does not exceed ten feet, the courses varying from one to two
and a half feet. None of the layers are continuous of the same thickness: sometimes a thick
one thins out entirely, and its place is taken by two thin ones; or a thin layer in one place
LIVINGSTON COUNTY. - & 461
becomes a thick one at a few rods distance. Sometimes the courses are separated by a thin
irregular course of hornstone; at others, this hornstone is in the centre or near the surface of
a layer of limestone. -- -
From Christie's quarry the limestone pursues a northwesterly direction, passing just to the
south of Caledonia village; it crosses the road a little west of that place, and pursues the same
direction to the top of the terrace on the south side of Allen's creek. West and northwest
of Caledonia, large numbers of fossils are found in this rock. In this part of the town, the
lowest portion of the rock is thick-bedded and compact; above this it contains a large pro-
portion of hornstone, and in some places is composed almost entirely of that substance. Being
in irregular shaped masses, and surrounded by limestone, which decomposes on exposure, it
is left scattered over the surface in rough and shapeless forms. These fragments are crossed
in every direction by innumerable fissures, which are expanded by freezing water, and the
whole falls into small fragments, which, in many places, literally cover the surface for many
acres. Where the road crosses this part of the rock, it has the appearance of being made in
a bed of flints. - - --
From the jagged and irregular appearance of the hornstone rock, as it occurs in detached
masses, it has received the familiar and expressive name of “chawed rock.” This rock is
the best material for road-making which Western New-York affords. Where it approaches
the surface the soil is rather barren, producing only a growth of dwarf oaks; but where there
is a tolerable proportion of finer materials, it produces a fertile soil. A large proportion of the
native growth along this terrace consists of oaks. -
Marcellus Shales.—The limestone is succeeded by the “Marcellus shales.” These shales
possess their usual essential characters; the middle portions quite compact and highly bitumi-
nous, becoming more slaty above and below. The compact part of the shale usually contains
large septaria; these sometimes consist of large silico-calcareous masses, without seams of
crystalline matter. This rock follows the same course as the limestone: commencing on the
east near the north line of the county, it passes southwest to the Genesee river; thence its
course is northwest through Caledonia, passing into Genesee county near the north line of this
toWn. - - -
On the Conesus outlet, near the lower saw-mill at Avon, this shale may be seen resting on
the limestone. About thirty-five feet from the bottom of the shale there is a stratum of lime-
stone one foot thick, sometimes concretionary, and containing Orthoceras, fragments of trilo-
bites, etc. For several feet below this, the rock is black, slaty and very fragile. A few feet
of the shale above this limestone is black and slaty; it abounds in fossils of Orthoceras,
Orthis, Strophomena, Avicula, and a very small species of Orbicula. Above this the mass
graduates into a greyish or bluish grey slaty shale, and contains few fossils.
This shale is seen in the ravines and hill-sides on the west side of the Genesee, extending
through the northeast corner of York, and thence through the southwest part of Caledonia.
At one place in the south part of this town, a digging for coal has been made in the black
shale. The indications which induced the undertaking at this place were the black and highly
462 GEOLOGY OF THE FOURTH DISTRICT.
bituminous character of the shale, thin seams of coaly matter and petroleum. I did not learn
to what depth the excavation extended, but presume it to have been less than forty feet, for
at that depth the Onondaga limestone would have been reached. The excavations were made
at two places, one on each side of a small shallow valley which was originally worn in this
shale. North of the valley, on the farm of Mr. M'Lean, the same shale was penetrated in
digging a well. Some portions of the rock are so highly charged with bitumen as to burn
when thrown into a hot fire. In these shales, as well as in the upper Genesee slate, nume-
rous excavations for coal have been made, and, in each, alike fruitless.
The Hamilton group is exposed in numerous localities in this county, and is everywhere
highly fossiliferous. Their destruction has afforded the highly fertile argillaceous soil which
is every where so productive of wheat in this part of the State, and perhaps nowhere more so
than in this county, •
On Jacock's run, the Ludlowville and Moscow shales can both be seen, separated by the
thin mass of crinoidal limestone. Here as elsewhere in the district, the Moscow shale is
known by its fossils, the Calymene and Cryphaus; while the Ludlowville shale contains
Atrypa concentrica, and large numbers of Cyathophylli and other corals. These fossils are
very characteristic of the two shales; still in some localities the Cyathophylli and smaller
corallines occur in the Moscow shales, but are not characteristic of this mass. -
At York, the Ludlowville shale is exposed on a small stream near the village; the fossils
are chiefly Cyathophyllites and Favosites, both in great perfection and beauty. Among the
former there is a specimen placed in the State Collection, consisting of twenty-six individuals
of the species turbinatum ? all closely grouped together. In the same ravine, several hun-
dred feet lower, may be seen the hard calcareous shale, or shaly limestone, mentioned in the
Report of 1839, as occurring at Tyler's on Seneca lake, and at Orleans in Ontario county. At
several other localities, these shales may be seen; but being of little economical importance,
they are described elsewhere. -
At Moscow, the locality which gives name to the upper member of this group of fossiliferous
shales, they are exposed in great perfection, containing abundance of the characteristic fossils.
These are the Calymene bufo, Cryphaeus calliteles, Atrypa affinis, and two or three species of
Delthyris. The principal locality is in the beds and banks of Beard's creek, on the land
of Jerediah Horsford, Esq. More than fifty species of fossils have been found at this place.
The Moscow shale is also exposed in a ravine, and the bed of a small stream, near the resi-
dence of the Hon. G. W. Patterson. These localities are in a deep valley of denudation, and
much below the general elevation of the surrounding country, the surface of which is occu-
pied by the Genesee slate. -
Genesee Slate.—In the ravines both east and west of Moscow, we find the Genesee slate;
also in a hill crossed in going from Moscow to the new bridge across the Genesee, and in the
hill side ascending from the valley to Geneseo. The same shale is seen in Fall brook, where
LIVINGSTON county. 463
the water leaps a hundred feet from the top of this rock. It underlies the village of Geneseo,
and is seen in many places on the road east from that place, and in the ravines between it and
Conesus lake. In this neighborhood the black shale is succeeded by a thin stratum of impure
limestone, which has been burned for lime at one place near Moscow. -
At the bridge crossing the Genesee near Mount-Morris, the Genesee slate is exposed, pos-
sessing all its essential characters; being bituminous, containing thin seams of coal, great
numbers of septaria, sometimes irregularly scattered, at other times in regular courses.
The arrangement and distribution of these septaria depended upon the supply of material;
and the tendency to concretionary forms proceeded from the amount of material being too
small for a continuous stratum, which, together with the homogeneous state of the particles,
caused them to take this form. Sometimes we see a single insulated mass, and no others in
the same parallel of stratification; at other times we find them distant from each other, but in
the same plane of stratification. Again we may find a course of them in the same plane, and each.
of them separated only a few feet from the other. Still again when the supply was greater, we
find a continuous stratum or bed, as in the case on Seneca lake, where the regular course of
septaria in the upper part of the black shale becomes, from increase of material, a continuous
stratum three or four feet in thickness. This change is seen in many cases near the thinning
out of a mass; the supply of matter diminishing, till it is traced only by distant nodules or
concretions. - -
The Cashaqua shale, for one hundred feet in thickness, is exhibited at the gorge at Mount-
Morris, limited below by the Genesee slate, and above by the Gardeau flagstones. It also ap-
pears in many ravines in the south and southwest part of Leicester; in the vicinity of Mount-
Morris; in the Cashaqua creek, whence it takes its name; in the ravines on the east of the
valley, and at a higher elevation southeast from Geneseo and approaching nearly to the
village. * - 2- - - -
The Gardeau and Portage rocks already described, are the southern rocks of the county.
These are seen in the deep gorge of the Genesee, and in almost all the ravines and water
courses of the southern towns. Among numerous localities as we approach Dansville, may
be mentioned Stony brook in Sparta, where several hundred feet of these rocks are exposed.
The shale in the upper part of this ravine has been ground and used as plaster.
There are several quarries between this place and Dansville, in which it is difficult to find
any characteristic fossils. The rocks consist of thick layers of sandstone, with intervening
masses of shale; and near Dansville, give more marked evidence of the group to which they
belong. Quarries have been opened on both sides of the valley, where materials were
obtained for locks, bridges, etc. on the Genesee valley canal. This group also affords the
finest flagging stones in the district; these are known by the presence of the fucoids already
mentioned. - - *
The great marl deposit of Wheatland extends into the northern margin of this county;
there is also an extensive deposit of marl about one mile east of Caledonia.
The Gardeau slide, which occurred more than thirty years since, still presents an interest-
464 GEOLOGY OF THE FOURTH DISTRICT.
ing appearance. The surface covered is several acres, and the clay is piled up in little
mounds and hillocks, with depressions between them, much in the same manner as the drift
hills of Ontario, and other parts of the district. Over a great portion of this surface no trees
are growing, and in some places even grass scarcely grows upon the clayey slopes. On the
opposite side of the river there is evidence of a former slide, even much more extensive than
this one, but the uneven surface has become overgrown with a heavy forest. The Gardeau
slide carried an immense body of earth into the Genesee river, which changed the direction
of the channel to the other side of the valley. These slides are but miniatures of those which
occur in the high primary mountains of the northern part of the State.
GENESEE COUNTY.
In this county we find the same rocks as in Livingston, with the addition of the Onondaga salt
group on the north, which extends through the towns of Bergen, Byron, Elba and Alabama,
and into the northern parts of Leroy and Stafford. - -
The most northern portions of this mass consist of greyish or greenish-grey marl, homoge-
neous in texture, and very compact when first exposed, but crumbling rapidly. Thin courses
of reddish and chocolate-colored marl are seen in some places in the northern part of the
county. Farther south, and along the centre of these towns, it is more grey or ash-colored,
contains thin seams of fibrous gypsum and selenite, and occasionally small masses of granular
gypsum. This part of the mass is exposed only in wells, which, from the difficulty in obtain-
ing water, are often dug to the depth of seventy or eighty feet. The grey marl and gypsum
is found to contain large seams or joints apparently water-worn ; these without doubt act as
drains, and carry off the water from above.
Some wells in this part of the group yield an acid water. One of these, belonging to Mr.
Gifford, of Bergen, I examined; the water is said to contain acid enough to curdle milk;
and though not sensible to the taste, is considered unfit for use. The famed acid spring in
Byron rises from this rock. Some of the wells in the immediate vicinity, and in the same
formation, yield good water.
A little north of Bergen centre the greenish marl comes to the surface, and is excavated
for the passage of the railroad. Two miles west of that place, the same marl is seen in the
roads and in the banks of the small streams, and approaches the surface over the greater
part of this neighborhood. -
The grey or ash-colored marls just described, are succeeded by bluish, slaty and drab colored
impure limestones, which embrace large beds of gypsum. These occur mostly in the north
part of Leroy and Stafford. Gypsum is also found in the western part of Elba, near the
junction of the Pine-hill road with the Batavia and Lockport turnpike, which is the most
GENESEE COUNTY. 465
northern point that I have found it, in the county. At this place some thirty or forty tons were
quarried; but the masses being small, and about eight feet below the surface, requiring the
removal of all the superincumbent earth and stone, the work proved unprofitable, and was
abandoned. - - - - - - -
In the vicinity of this quarry, and for some distance west, there are sufficient indications
of gypsum in the peculiar irregularity of the surface, which is raised into little mounds,
giving it the appearance of heaps of earth deposited on the level soil. The thin bluish or drab
limestone is also found near the surface, and often ploughed up in the fields.
In the north part of Leroy, plaster is obtained in large quantities, on lots 118, 144 and 132.
The quarries in the first are of white gypsum, free from seams and intermixture of clay; it is
covered with a bluish kind of limestone with shaly seams, and which separates into laminae
one-fourth or one-half an inch thick. In the others, the gypsum is clay-colored, with seams of
clay; this, when exposed, crumbles rapidly. The rock above is a drab limestone, resembling in
general appearance the hydraulic limestone. In this I found some few fossil shells of a spe-
cies of Avicula. Some parts of the rock are filled with small round pores, the size of a mustard
seed; such are also seen in the soft limestone, a few feet below the hydraulic or drab lime-
stone. The masses of gypsum are all more or less spherical; the surrounding rocks being
raised in the centre, presents a fractured convex surface, dipping on every side.
The quarries last mentioned, belong to Messrs. Bannister, Collins and Clifford; the white
gypsum to Mr. Hughes and Mr. Cash. The plaster is sold at the bed for fifty cents, and
when ground, from three dollars to three dollars and fifty cents per ton. The different beds
in this county furnish about three thousand tons annually. -
The formation described, belongs apparantly to the second or middle series of gypsum beds;
the upper, like that at Seneca-falls and Vienna, is not seen, neither have I been able to find
the lower series; but although similar in general character, it would appear that the white
gypsum above described, which is half a mile north from the others, must be at a different
elevation, as well from its position as from its associated rocks. The general direction of the
masses is N. W. and S. E., as appears both from the beds here, and from their reappearance
in the western part of Elba. * . -
The alluvial excavation along the valley of Black and Bigelow Creeks, has either removed
the gypsum, or covered it so deeply with drift that it is not reached in ordinary excavations;
but unless so removed, the whole distance across the country is probably underlaid by it,
though its depth may be too great for profitable exploration. *~. -
The gypsum is succeeded by various colored marls, mostly bluish, greenish and drab or
ash-colored; some hard and very calcareous; others soft, crumbling, and forming a tenacious
clay. - -
The drab limestone, or hydraulic limestone, is the next succeeding mass. The essential cha-
racters of this rock have already been described ; its thickness is variable, and also the pro-
portion of sand, clay and carbonate of lime. Its connexion with the Onondaga limestone
above, is seen to advantage at the falls on Allen's creek, two miles north of Leroy; and also
[GEol. 4th DIST.] 59
466 GEOLOGY OF THE FOURTH DISTRICT.
at Morgansville, where the Black creek descends from the limestone terrace to the level of the
country north. The section at this place is given on page 140 of this report.
This rock forms the northern escarpment of the great limestone terrace, extending from the
Genesee to Lake Erie, and is also seen in the counties east. It passes through the towns of
Leroy, Stafford, Batavia, and the south part of Alabama, forming the lower falls on the
Indian reservation. I am not aware that it has been used for cement in this county, though
it is doubtless good for this purpose.
The Onondaga and Corniferous limestones occupy the summit of the terrace; extending
from Livingston county westward; pass with variable width to the north of the village of Leroy;
underlying Stafford, Morganville, the north part of Batavia and Pembroke. A few feet of the
lower portion of these rocks is in regular courses, with little or no hornstone; the succeeding
forty or fifty feet consists principally of hornstone, being a rough ragged mass, called the
“chawed rock.” This, in some places, contains large numbers of corals.
About two and a half miles north of the village of Leroy, and west of the creek, thereis
an extensive quarry in the Onondaga limestone. The rock at this place appears in courses,
varying from six inches to two feet; it is almost wholly composed of fragments of Crinoidea and
other fossils, crystalline in texture, quite tough. The thick courses are often divided by seams:
these, when of clay, cause the blocks to separate ; at other times they produce no injury.
From the quarry, the rock is taken to a mill a mile south of the village, and sawn into slabs
and blocks; it is afterwards polished and used for fire places, mantle pieces, etc. The
polished stone has often a very beautiful appearance, and is highly prized by the collector,
on account of displaying the internal structure of fossils cut through in the process. The
crinoidal joints are frequently of a different color from the surrounding mass, a variety which
increases the beauty of the stone. } -
Lime is burned at many points along this range, supplying the immediate neighborhood,
and also the country north and south. In Stafford, Batavia and Pembroke, this rock appears
in numerous localities. Two and a half miles from Batavia village, and half a mile from the
north hine of the town, the rock exposed is the hydraulic limestone, with some thin layers
above, and the greater part consisting of the “chawed rock.” This latter is most annoying
to the farmer, and when it overspreads the surface in large masses, almost totally forbids
cultivation. This is seen in several places of small extent, in the south part of Alabama.
The growth of timber on such land consists chiefly of oak. “r. - -
On the Indian reservation, this rock appears at the upper falls, and in the stream below;
also between this and Pembroke. The thickness of the mass is very variable, as may be
seen in the quarries, where thick masses at one place may be merely recognized in another
by layers of a few inches. West of Batavia the terrace is not so well defined, though there
is little difficulty in tracing the course of the limestone.
The shales above the limestone are seen to less advantage in the county of Genesee than
in any other of the same range. At Leroy the Marcellus shale succeeds the limestone, and
is well exposed in the bed of the stream at that village. It contains large masses of septaria,
GENESEE COUNTY. 467
which are more calcareous than those of this shale in most places. The compact portions of
the shale have been quarried for firestones; and the black stone store in this place is built of
the same material. -
Farther south, we find the lower members of the Hamilton group at Clifford's mill at Roan-
oak, and a little north, where it consists of those portions that are nearly destitute of fossils,
and consequently of less interest. In the Four-mile creek near Roanoak, the same shale is
SCCI1, - i -
The shales of this group are found in two or three places in the town of Covington: one
of these is a mile north of Pavilion; and another, one mile and a half southwest, in the bank
of the creek near Sprague's mill. The rock in place is scarcely visible at either of these
localities; at the first it appears as a bank of clay, produced by the decomposition of the
mass, leaving the fossils. This clay is used for bricks. At the latter, the decomposing edges
of the strata are covered with gravel, the fossils being washed out by rains.
At one or two places near Bethany centre, the upper shales of this series are seen; and
near the village of Darien, on the Eleven-mile creek, there is a natural section showing the
Ludlowville shale, the Crinoidal limestone, the Moscow shale, and near the same place the
Genesee slate. The Ludlowville shale contains its usual fossils, Favosites, Cyathophylli, &c.,
the Atrypa concentrica and A. affinis, Delthyris and Strophomena. The crinoidal limestone
has fewer fossils than usual, but the Avicula is numerous. The Moscow shale appears much
thinner than elsewhere, and exhibits fewer fossils. -
The next range of towns south, as well as a great portion of Sheldon, Orangeville, War-
saw and Perry, are occupied by the Cashaqua shale and the Gardeau rocks. The southern
towns, with the more elevated portions of the range next north, are underlaid by the Portage
rocks, and in Arcade we find the commencement of the Chemung group. - -
In passing south through the towns of Darien, Bennington, Sheldon, &c., we find that the
rocks (mostly shale) lie near the surface almost continuously, except in the valleys. Plough-
ing often turns up the black or the green Cashaqua shale, and the road sides expose the same
at frequent intervals. These shales are left in little eminences above the general level of the
country, and being covered with alluvium, are often mistaken for alluvial hills; whereas the
soil is thin, and the removal of a few inches frequently exposes the rock. These knolls are
seen along the road south, from Long's corners through Darien to Bennington. This condi-
tion of the surface, previous to the deposition of the alluvium or drift, appears to have resulted
from the action of the waters of a lake or ocean, where numerous currents and counter cur-
rents might wear away the intervening masses, leaving the projection of the little mounds of
shale as we now see them. - -
In several places slight “diggings” have been made, upon the indications of some thin
seams of coal. Three miles south of Wyoming or Middlebury there have been excavations
at two points, and at one of these a boring of thirty feet. At the time I examined the place,
the owners, Messrs. Marvin and Joseph Everest, were about contracting for a deep boring, in
the sanguine expectation of finding coal. -
59*
468 GEOLOGY OF THE FOURTH DISTRICT.
In the ravine west of Warsaw, some of the Gardeau rocks are exposed; and in the ravine
southwest of the village are found rocks of the upper part of the Portage group, though
mostly destitute of the characteristic fucoid. In this ravine there is a waterfall of one hundred
and ten feet, which, together with the rocks above and below, gives a thickness of two hun-
dred feet at this place; they are principally shale with thin layers of sandstone. -
The upper part of this group may be seen at the falls on Allen's creek, near the north
line of Gainesville, and about three miles south of Warsaw village. On elevated ground from
Sheldon to Warsaw, this mass, with its vertical fucoid, appears in several places along the
road. - ~ . ". -
The swamps in this county containing muck, are exceedingly numerous. This deposit, in
the Fourth geological district, has in but few instances become sufficiently tenacious to be
called peat; though it burns as readily, and is equally good for fuel; but in drying, it falls to
powder. In many places, when the swamps shall have been drained, and time allowed for
the muck to become more compact, and other vegetation to succeed the present, many of
these deposits will furnish valuable fuel. -- -
Near Batavia, several small swamps or ponds contain marl, and also the springs or ponds at
the source of Spring creek. About three or four miles north of Leroy, between the gypsum
beds and Bergen, there is a large marl Swamp ; the extent of the deposit I did not learn, but
it is probably great, resulting as it does from the marls and slates of the gypseous formation.
Two and a half miles south of Leroy, on the land of Archibald Stewart, and an adjoining
farm, a marl bed covers about twenty acres, with an average depth of probably eight feet; a
few rods from the margin being five, a little distance farther nine, and the centre fifteen feet.
This marl is covered by muck, from one to two feet thick. Mr. Stewart has applied the marl
as manure, and finds ample returns. -
In examining Silver lake, I found the bottom in many places covered with a growth of Chara,
which, when first thrown out, looks green, but on a little exposure it becomes white and brittle,
readily crumbling to powder; they are almost wholly composed of carbonate of lime. The
same species is found abundantly in the outlet of the Caledonia spring; and so rapid is its
growth, that frequent removals are required to prevent it from impeding the water in the
sluiceways to the mills. Towards the inlet, the bottom of this lake is covered with marl
several feet deep, but I was not able to ascertain whether it occupied the whole area. From
sounding, the bottom appeared soft. The marsh at the head of the lake was not examined,
though it probably contains marl. - 2.
In all deposits of tufa and marl, a large quantity in the bottom of the bed is earthy, and
considered unfit to burn for lime ; these portions, either in their actual state or burned, can be
advantageously used for agricultural purposes. Lime burned from this, and made into a com-
post with the black muck of swamps, would be an excellent manure for all the lands of the
southern counties; and even the hardpan, which is considered almost worthless, may be
reclaimed, and rendered fertile by the judicious application of muck and lime. The impor-
tance of this subject cannot be too strongly urged. While the farmer is perhaps cultivating a
ERIE county. r 469
poor, hard soil, too compact for vegetable growth, his lands include a muck swamp, which
is considered nearly worthless. Now, by ditching this swamp, and carrying its contents into
his fields, both are essentially improved. The soil of these swamps, when reclaimed, is Supe-
rior to the higher grounds. 2 .
ERIE COUNTY.
The lowest rocks of this county are those of the Onondaga salt group, which are succeeded
by the hydraulic limestone, the Onondaga and Corniferous limestones. The central part of
the county is occupied by the Marcellus shale and Hamilton group, while the rising ground to
the south is formed of the rocks of the Portage group. - .
The Onondaga salt group occupies all that low ground on the north of the limestone terrace,
which is generally designated Tonawanda swamp. The greater part of this portion of country
is, however, very far from being a swamp, and at present the term may be applied only to
that portion bordering the creek. Even here, too, its necessary condition is not a swamp, but
requires only proper drainage to convert it into excellent agricultural land. -->
From the ancient condition of this part of the county, and the deep deposit of drift, the
rocks appear but in a few places, and these only for a small extent. The principal place is
in the bed of a stream on the farm of Mr. Martin, in the north part of Clarence.
The rock seen here is that portion containing small cavities of the size of flax seeds, often
running together, forming linear ones; and in a few cases, the hopper-shaped cavities were
observed, though the rock is usually quite solid and firm. Where the rock is penetrated beyond
the influence of the weather, these cavities are filled with plaster. The portion of the mass
here exposed is concretionary. No plaster, or even any evidence of it, appears at this place;
the mass in question, however, is apparently that which has before been found, separating the
upper from the next lower course of gypsum beds.
The shaly and marly portions of the group are met with in digging wells, generally from
ten to twenty feet below the surface; in some places they are not found at all, and it becomes
quite difficult to obtain water at the ordinary depth of wells. -
From this fact we perceive, that a search for plaster, however successful as to the discovery,
would be of little benefit, owing to the great depth below the surface, which would not allow
of its being raised at the present prices. That the plaster exists, is very probable; for there is
nothing in the character of the rocks, or of the plaster in the western part of Genesee county,
which indicates that it disappears farther west. Plaster is also obtained on the Grand river in
Upper Canada, forty miles west of the Niagara. A great portion at least of the intermediate
space between the two rivers is in a similar condition to the country along the Tonawanda
creek.
470 * . GEOLOGY OF THE FOURTH DISTRICT.
Thus far no excavations have been made in search of plaster; and in digging wells, I am
not aware that it has been seen. Neither is it probable that such would be the case; for I
am informed, that soon after coming to the rock, water is found; and the object of search thus
obtained, nothing else is thought of. Should the value of plaster increase with the exhaustion
of the beds farther east, we may then expect that search will be made for it in this region;
and when the price is such as to repay its being raised from fifteen to thirty feet below the
surface, we shall in all probability find a sufficient supply in this county for a long period.
The surface of the country north of the terrace is level, or gently undulating; the inequali-
ties are caused by the accumulation of gravel or sandy loam, the latter often covering gravel.
The soil for the most part is loamy, of a yellowish or brownish color. A few inches of the
surface is usually blackened by vegetable matter; sometimes the loam becomes stiff, from
admixture of clay, and at other times it is mixed with fine gravel. In the lowest grounds the
soil is clayey; often a stiff white or bluish-white clay, frequently stained with iron, at the
depth of six or eight inches. On this kind of soil we find evergreens. The clay or soil, in
such cases, seems to have been deprived of its coloring matter, which is iron, by the percolation
of water through the carbonaceous matter above. This solution and removal of the iron by the
carbonated water gives rise to the small beds of bog ore, so frequent in this valley. Where
the rock is near the surface, or the soil contains much lime, this also is dissolved, and we
have a deposit of tufa, charged with iron. Several of these beds have been met with, and one
of them, north of Clarence-hollow, was formerly supposed to be valuable. There is not,
however, sufficient iron to be of any importance, and the tufa is of no other use than for
burning into lime, * - -
From the generally even surface of this tract, we find numerous swamps, of small extent;
in these are valuable deposits of muck, which will always be available as a fertilizer of the
soil, more particularly the clayey portions, which require vegetable matter to render them
lighter and easily worked, as well as more productive. -
The hydraulic limestone follows the course of the terrace, lying at its base, or outcropping
along the northern slope. It is characterized here, as elsewhere, by numerous and copious
sulphur springs. These are generally to be found near the base of the terrace, or within a
mile to the north. Near the eastern edge of the county, this limestone is developed in its
entire thickness at the falls at Falkirk. The upper portions are extensively quarried and
burned for cement. It possesses all the essential characters of that from Onondaga and
Williamsville. The outcrop of the mass may be traced from hence westward, along the slope
of the terrace. At Clarence-hollow it has been quarried and used in building. At Williams-
ville, it is extensively quarried by J. S. King & Co., and burned into water cement. There is
made at this place annually from forty to fifty thousand bushels, or ten to twelve thousand
barrels. About three feet of the upper part are unfit for burning, being too calcareous; below
this there are four feet of good quality, and then a shaly mass of two or three feet thickness,
below which the rock is fit for cement. The facilities for quarrying and grinding the cement
are here very great, the Ellicott creek descending from the summit of the terrace at this
ERIE COUNTY. 471
place. Care is required in selecting the rock as it is quarried, thin seams of shaly matter
intervening between the thicker masses, which only are fit for cement.
The next place west of Williamsville where this rock is exposed to any great degree, is in the
Skajockety creek, about four miles from Buffalo. Here there are about twenty feet of the rock
visible, extending for half a mile north of the road. The upper portions abound with cavities,
many of them containing sulphate of strontian, but principally empty, and showing the re-
mains of a small coral which has been partially removed. Below this the mass is quarried
for rough building stone, in blocks from four to eight inches thick; thin layers are often quar-
ried for flag-stones and door steps. The rock has all the external characters of the water lime-
stone of Williamsville and Falkirk, and is probably as good for cement.
Between the place just mentioned and Black-Rock, the hydraulic limestone appears in
several places; the most prominent, however, is on the land of Mr. Arms, a mile and a half
east of Black-Rock, where large quantities can be easily obtained. The burning of the rock
at this place has been heretofore attempted, but unsuccessfully. -
At Black-Rock and the vicinity, the water-lime appears in several places. At the quarries
near the ferry, the rock is visible to a depth of eight feet, underlying the blue limestone.
Here, as at other places, the upper portion of the mass is too calcareous, and it is only the
ash-colored and striped layers beneath that are fit for use as a cement. The situation at this
place is very favorable ; but where covered by the other rocks, it cannot be profitably brought
into use. By pursuing examinations to the northeast of the village, the same mass may be
found covered only by the soil, and consequently much more easily obtained. r
In many places, and for the greater part of the breadth of this county, the Onondaga lime-
stone forms a very thin mass, or the limestone above rests immediately on the hydraulic
limestone. It is owing to the resisting nature of these two limestones, and to the soft nature
of the rock on the north, that a terrace is formed, leaving the valley of the Tonawanda ex-
cavated from the rocks below. The undulating outline of the terrace is also caused by the
greater or less thickness of the limestone. Sometimes we find it jutting out to the north a
mile beyond the general line, and again falling below or south of the general direction nearly
as far; the latter appearance usually occurs where the terrace is cut through by streams run-
ning to the north. . -
At Black-Rock, the Onondaga limestone is only from six to fourteen inches thick; it is of
a greyish color, crystalline, and containing few fossils. This mass has been quarried, pro-
ducing excellent stone for fine building or foundations. Some of it has been sawed and
polished, being sufficiently compact to form a good marble; the colors, however, are dull.
The Corniferous limestone is extensively quarried at Black-Rock for the public piers, break-
waters, etc., and serves a very good purpose where rough stones are required. From its posi-
tion, and its vicinity to the public works and canal, it becomes invaluable to the State.
The hornstone portion is largely quarried for use on the Macadam road, and is an excellent
material for this purpose; the hornstone, from cracks and fissures, readily falling to pieces by the
action of frost, produces a bed of angular fragments little affected by the changes of weather.
472 GEOLOGY OF THE FOURTH DISTRICT.
In the town of Newstead, a mass of partially decomposed clay and sand lies between the
water-lime and Onondaga limestone; it is about six inches or a foot thick, highly stained with
iron, and exhibiting a partially conglomerated appearance. In this are several peculiar coral-
line fossils. It occupies the place of the Oriskany sandstone, and is its only representative.
The demand for lime in the city of Buffalo, renders the existence of this limestone range
of the greatest importance to the inhabitants. There are burned annually, in this county,
from 27,000 to 30,000 bushels of lime, and this amount is greatly increased in times of com-
mercial prosperity. - - - - - -
The kilns at which this lime is made, are nearly all situated between Clarence-hollow on the
east, and three miles west of Williamsville. Along this distance there is a thick mass of lime-
stone free from hornstone, consisting principally of grey crystalline rock, filled with crinoidal
joints and other coralline remains. - -
The great accumulations of drift upon the southern slope of the terrace prevents, for the
most part, the examination of the shales above the limestone. It is only in a few places along
the Eleven-mile creek and the Cayuga Creek that they can be seen; and these exposures are
very partial, and would lead to little information concerning the rocks, did we not know their
character at places farther east. '- . -
Following the latter stream below Alden, we trace its course in a deep alluvium, till near the
line between Alden and Lancaster, where it crosses the limestone which is exposed by the
creek for a considerable extent. The shales are slightly seen in several places on the Cayuga
creek, but the banks almost continuously are of alluvium, from ten to twenty feet in depth.
The junction of the Little Buffalo with the Cayuga creek exhibits the calcareous mass, which
separates the upper Marcellus from the shale above. The lower Marcellus shale is seen at
only one place on the Cayuga creek, and here only in the bed of the stream.
On the Seneca creek, and the Cazenovia creek, on the Indian reservation, these shales oc-
cur; and here we find them much better developed than elsewhere in the county, except on
the lake shore. Near the Indian council-house on the Cazenovia creek, appears the lime-
stone separating the upper and lower Marcellus shales. It abounds in a trochus-shaped
fossil, and in fragments of Orthocerae. This is the only place, so far as I know, where this
mass is visible in Erie county. The lake shore, for eight miles above Buffalo, exhibits no
rocks; the whole country is low and nearly level, constituting what was formerly designated
“the swamp.” - - t
At Comstock's tavern, the shale appears for the first time on the lake shore. Beyond this,
the shale becomes more fossiliferous, containing Delthyris, Atrypa, Strophomena, Calymene,
etc. These increase in numbers as we ascend, and finally in many places the rock is com-
pletely loaded with them, particularly at Eighteen-mile creek. 2--- t
The Encrinallimestone, below the Moscow shale, is here avery distinct stratum; and being
undermined by the action of the waves, it falls down in large slabs, which furnish a very good
building and foundation stone. - -
The under side of this limestone is covered with a coating of iron pyrites, which has been
wrought to some extent, on the supposition that it was silver.
ERIE COUNTY. 473
The only representative of the Tully limestone is a layer of argillaceous, often concretionary
limestone, about three inches thick, succeeding the Moscow shale. --
The Genesee slate succeeds the Moscow shale, and is found near the limit of the county,
on the Eleven-mile creek; it appears also on Cayuga creek, lot 30, town of Wales; again,
at Hatch's mill on the Seneca creek, Indian reservation; and also on Cazenovia creek, near
Aurora, and is barely visible in many other places in the small streams. It every where pre-
sents its usual character of black, slaty shale, and is every where marked by the presence of
Avicula fragilis. Its first appearance on the lake shore is in a high bank, twelve miles from
Buffalo, forming about six or eight feet of the upper part of the rock; beyond this it is not
seen till after passing Eighteen-mile creek, where its whole thickness is visible, lying between
the Moscow and Cashaqua shales. It disappears beneath the lake, nearly two miles south-
west of Eighteen-mile creek. - - º
In Erie county, the Cashaqua shale is seen in the Cayuga, Little Buffalo, Seneca and Ca-
zenovia creeks; also in the banks of Eighteen-mile creek, extending for two miles or more
from the lake. Southwest of the mouth of Eighteen-mile creek it appears in the high bank,
exhibiting its whole thickness. It is of a greenish color, embracing numerous courses of
irregular, flattened concretions, consisting of clay and sand, with some carbonate of lime.
These masses are the only representatives of the continuous layers of calcareous and argilla-
ceous sandstone, which occur further east. This shale forms a very tenacious, clayey soil,
as is well seen after ascending the hill beyond Eighteen-mile creek, where the soil is almost
entirely formed from this rock. It disappears near Lay's tavern, three miles southwest of
Eighteen-mile creek. - -
Above the Cashaqua, we find black and dark colored shales; and to these succeed alterna-
tions of dark green and black shales, the green portions often predominating for miles, and
the whole extending beyond the county line. These are all destitute of fossils, except occa-
sional traces of fucoids. The higher part of this group may be seen in following up the
Little Buffalo, Seneca, and Cazenovia creeks and their tributaries. The layers of sandstone
are thin, and afford good flagging stones; they are also used for other purposes. This group
occupies all the lower portions of the hills and moderately elevated grounds in the southern
part of the county. It can be seen to advantage at Griffin's mills, three miles south of Aurora.
Several of the thin layers of sandstone alternating with shale are seen in a small stream one
mile east of Aurora. - - - r
Several quarries are opened near Boston centre, where the flagging stones of this group
are quarried. The slabs are from one to six inches thick, and separated by joints of eight feet
by six broad; some are fifteen or twenty feet in length.
The rocks of the upper part of the Portage group occupy the highest grounds of the
southern part of Erie county, frequently outcropping on the small streams and ravines. The
sandstone of this group is thin, compared with the same farther east, and there are but few
quarries opened. - º
About two miles south of Aurora, the higher rocks of this group are quarried by Mr. Treat
[GEoL. 4th DIST.] 60 -* --
474 GEOLOGY OF THE FOURTH DISTRICT.
and Mr. Jones; they are here characterized by a fucoid vertical to the strata. Half a mile
east of Griffin's mill, the same mass is quarried by the road side. w
On lot 22, six miles west of Springville, on Mr. Pack’s farm, two quarries have been opened
in this rock. There are also two other quarries about one mile north of Springville. The
stones from all these are usually thin, though affording good material for ordinary building
purposes. - *
This group commences at the ascent south of the Indian reservation. The thicker sandy
portions occupy the brow of the hills or most elevated situations, while the whole slopes off to
the north in proportion as the hard layers diminish. Thin flag-stones and building stones are
obtained from the upper part of this group everywhere in the county south of the Indian
reservation. - *-- - --
The soil between the top of the limestone terrace and the Indian reservation on the south,
is for the most part a gravelly loam, though in many places it possesses different characters;
towards the Niagara river, in the lower grounds around Buffalo, the soil is clayey. For some
distance east of Buffalo, and particularly near the creek, it is a clayey loam, being adhesive
when wet, but readily crumbling when dry.
Along the Cayuga Creek, in many places, there are deep accumulations of gravel. When-
ever the shale approaches the surface, it produces a clayey soil; but this is a small proportion
of the whole, which is mainly of materials from farther north, as limestone, sandstone and
argillaceous matter from the salt group north of the terrace. On the north side of the creek,
in the towns of Alden and Lancaster, a deep gravel deposit extends for several miles. In
its eastern termination it is more loamy, and the soil south of the creek possesses the same
character, or becomes clayey. For the most part, the soil along the outcrop of the black shale,
and for a little distance north, is clayey; but this is often concealed by the gravel deposit.
The present stream runs in a narrow channel with a gravelly bottom ; from four to ten feet
above, a level bottom land spreads out on both sides for a quarter to one mile. This
bottom is composed of fine loam, and evidently has resulted from quiet waters, both from its
nature and its evenness. The sides of these flats are terminated by banks from fifteen to
thirty feet high, sometimes rising gently, at other times abruptly. These banks, which appear
to be the limit of the former stream, or estuary through which a stream flowed, are of mixed
materials, coarse and fine gravel, sand and loam. The general character of the soil of these
high banks is gravelly, and its extent on either side of the creek is variable. Sometimes,
beyond this there is a second ascent or terrace, particularly where we come into the region
of the rocks above the Genesee slate, and the sides of this are also covered with gravel to a
certain height. - - -
Round gravel, however, occurs but sparingly at an elevation much more than two hundred or
three hundred feet above Lake Erie. The soil above this elevation is of a different character,
being what is often and very expressively termed “flat gravel.” By this is meant, that
fragments of rock contained in the soil are flat and angular, having never been subjected to
a wearing action sufficient to smooth them. - - -
TOMPKINS county. 475
This kind of soil covers a large portion of the southern half of the county, more exclusively
the higher grounds; rounded and worn materials occupy only the valleys of the larger streams,
diminishing as we ascend from them. The “flat gravel” consists of the materials of the rocks
in place near, and appears never to have been transported to any great distanee. These rocks
consist of soft shale, argillaceous and calcareous sandstones; consequently the soil is of the
same nature, varying in proportion as the rocks beneath vary, sometimes more sandy and
at others more clayey. It may be described as a clayey loam, becoming tenacious when wet,
but not cohering when dry. The coarse materials consist mostly of argillaceous sandstones
in thin angular fragments, and in some places still undecomposed shale. The transported
materials in this part of the country are confined to those valleys which are connected with
others farther south, and through which the north and south current found an outlet. In this
soil there is a much larger proportion of lime, and we find it more productive of certain crops
than the higher grounds. The valley of the eastern branch of Cazenovia creek, and the northern
branch of Eighteen-mile creek, have a much greater surface covered with this kind of soil
than the others, and we find that these communicate more directly with the Cattaraugus creek
at the south. -
Along the Cazenovia and Seneca creeks, above their junction, there is much gravelly soil,
forming an almost level surface for considerable extent. This continues below the junction of
these streams on the south side, and is seen in isolated patches, mounds, and low ridges,
extending to the lake, four miles west of Buffalo. • :
The same soil is found along the Cattaraugus creek, and at about the same elevation above
the lake; it also occurs, in less extent, in several other places, and is characterized by a
growth of oak. It is evidently a deposit from coarse materials brought into the lake by
streams, and by the action of its waters spread evenly over the bottom. The same features,
to a small extent, are now to be seen on the shores of the present lake, where a large stream
flows into it. -
TOMPKINS COUNTY.
The northern part of this county, between the Seneca and Cayuga lakes, (being the wes-
tern half of the county,) is occupied by the rocks of the Portage group, with the exception
of the lake banks and the deep ravines of the same. In these situations we find the Genesee.
slate, the Tully limestone and the upper part of the Hamilton group, each one in its order,
disappearing beneath the lake level as we proceed southward. These rocks from the Tully,
limestone upward are well exhibited in the deep gorge of Halsey’s creek, below Taghannuc,
falls. The Genesee slate, which is visible for more than one hundred feet above the Tully lime-.
stone, is succeeded by nearly three hundred feet of the rocks of the Portage group, consisting in
60*
476 GEOLOGY OF THE FOURTH DISTRICT.
the lower part of a mass of siliceous shale, and above alternating with argillaceous sandstone.
The surfaces of this rock are often rippled, and covered with minute fragments of vegetables,
which seem to follow the course of the marking, and accumulate or diminish with the ripple
wave. The same appearance is presented by a beach of sand, where the ebbing tide leaves
fine fragments of vegetable matter arranged in quantity and direction proportionate to the
Wave. - - * - - - -
The Tully limestone and the shale below disappear on Cayuga lake, four miles from Ithaca,
the black shale extending about two miles farther south ; and on the western side of the
county, in consequence of the greater elevation of Seneca lake, the black shale disappears
near the southern boundary of Seneca county, with the exception of a small portion rising
above the lake, which results from the undulation farther south, The succeeding group of
shales and sandstones approaches the level of Seneca lake north of Hector falls, and Cayuga
lake near its head. -
The Chemung group, like the preceding, consists of alternations of shale, both slaty and
compact, and argillaceous sandstone, but differs from it in the contained fossils, and in some
particulars of its lithological character. It sometimes contains thin layers of impure lime-
stone, the calcareous matter arising principally from the contained shells. This group is well
characterized at Ithaca, at the inclined plane of the railroad; it extends also, far above the
rocks here visible, attaining a much greater thickness, as can be seen in the valley of Che-
mung, south of Seneca lake. In the rocks of this series, individuals of two species of ferns
have been found, precursors of the great abundance of that tribe in the Coal formation.
At Hector falls, and above, we find about four hundred feet of this group exposed; the
lower part contains the ferns of Ithaca ; and above, some of the other fossils. At this place,
we find a few thick layers of sandstone, very compact and firm, which have been quarried.
Few durable building stones are found in this county, if we except this sandstone, which,
however, is little used. It furnishes the fine flagstones used in Ithaca and elsewhere. In
general characters it differs but little from that of the group below, except that the casts of
mud furrows are more abundant and large, being often an inch in diameter and several feet in
length. The surface of most of the layers is smooth, or even glazed with a thin coating of
shale, which appears to have flowed over it, leaving marks of unequal deposition, and little
ridges or prominences where the paste was less fluid. The deposition of these shales and
sandstones progressed slowly, considerable time having elapsed between the deposition of the
different layers; and in some instances a lower stratum became partially indurated before the
succeeding deposit was made.
In some localities the sandstone is replaced by a kind of sandy shale, being a mixture of
sand and clay; and the whole is rippled, the markings affecting each thin layer, and showing
that it was deposited from water in motion which might transport from different directions the
two materials of the rock. This group appears to have been deposited from an ocean alter-
mately at rest, and disturbed. Thick masses of sandy shale occur, bearing ripple-marks
through their whole depth; these are succeeded by others of variable thickness, without ripple-
TOMPKINS COUNTY. 477
marks, and having the faces smooth and plain. Numerous alternations of this kind have been
noticed through many hundred feet. Fossils rarely accompany the rippled layers, but are
invariably found with the smooth. The materials of the two differ very slightly in mineral
composition, the rippled ones being more sandy. So far as I have observed in this and other
localities, the greatest accumulation of fossils is always accompanied by the fewest ripple-
marks. - - /
In numerous localities of these rocks, the edges of strata, when exposed in ravines and
other places, are found covered with crystals of sulphate of lime. This circumstance is by
no means universal among the shales below, although observed in some localities; while in
the present group there are few exceptions. Pyrites, in minute particles, is every where
disseminated, decomposing on exposure, and hastening the destruction of the rocks; while
the sulphuric acid combines with the minute proportion of lime which they contain, exhibiting
the crystals along their edges. Wherever larger masses of pyrites occur, we find a proportionate
increase in the quantity of sulphate of lime. Similar conditions in some of the limestones
below have produced a mass of gypsum, filling the cavity previously occupied by the pyrites;
and analogous circumstances, and varying in extent and effect, may have formed the vast
gypsum beds of the same series, extending throughout the whole of western New-York. The
latter, however, could only have occurred before the entire induration of the surrounding rocks.
The thin-bedded sandstones of this county afford some of the finest flagging stones observed
in this part of the district. These are quarried in large slabs, having a thickness of from three
to five or six inches. The thicker layers furnish a good material for buildings and foundations.
There are several deposits of marl in the marshy ground at the head of Cayuga lake, which
might be advantageously used for burning into lime. In the south part of the town of Hec-
tor, there is an extensive deposit which is already largely used for burning into lime. There
is another deposit in the same valley at Reynoldsville. - -
About six miles south of Ithaca there is an extensive bed, and several small ones near
Newfield.
CHEMUNG COUNTY.
The surface of this county is occupied by a series of broad high hills and deep narrow
valleys; the Chemung valley is an exception, however, being broad and deep, with an exten-
sive alluvial bottom. - * -
In the deep ravines of the northern part of the county, the rocks of the Portage group are
exposed; but nearly all the surface is occupied by the Chemung group, the characters of
which are already described. The rocks are deeply indented by numerous ravines which
expose the strata to great advantage, and offer facilities for exploring their fossil productions,
478 GEOLOt 'Y OF THE FOURTH DISTICT.
In the vicinity of Millport, and farther south, the sandstone layers attain a thickness of a
foot or more, and are quarried for works on the canal and various other purposes; and at
Pine valley, the sandy layers of the rock are quarried in two places. Mr. Sexton, the owner
of the last, informs me that the firmest layers of sandstone often pass into shale, so as to be
unfit for any useful purpose. This appears to be unlike the thinning out of the layer; but
the proportion of argillaceous matter becomes so great that the mass crumbles on exposure.
At Maybee's quarry, a mile and a half east of Horseheads, the rocks are quarried for the
sandstone which is used for flagging, step stones, etc. These layers are highly siliceous and
compact; and sometimes contain a few fossils. They alternate with thick masses of shale;
often several layers of the former separated by thin seams of the latter; and again, a thick
mass of shale containing no sandstone. A similar quarry has been opened by Mr. Tuilegar,
four or five miles east of Elmira; here the layers are very uniform, from half an inch to two
inches thick, and dividing by the vertical joints into slabs from six inches to two or three feet
wide, and from four to six feet long. The sandstone contains a few specimens of Atrypa, but
the greater proportion of fossils are found in the shales. Wisner's quarry, near the village
of Elmira, is in a lower position in the group, and the rocks are almost destitute of fossils.
The rocks of this group, containing an abundance of fossils, occur on a small creek coming
into the Chemung valley from the northwest, and also on the Singsing creek, passing through
Bigflats. On the south side of the Chemung river, in Southport, the banks of the valley
exhibit the rocks of this group with their peculiar fossils.
Between Elmira and Chemung they are seen at numerous points, but nowhere in the county
so well as at the Chemung upper narrows, about eleven miles below Elmira. Here the exca-
vation for the road along the margin of the river has exposed more than one hundred feet of
rocks, containing abundance of the characteristic fossils, and in their greatest beauty and per-
fection. At a certain point in the mass exposed, we find a peculiar coralline fossil, confined
to a thin stratum, and extending along the whole distance of the exposed rocks; it has also
been found at other localities.
The mountain above the rocks exposed, at Chemung narrows, rises four hundred or five
hundred feet, and is probably capped, as some of the hills in the neighborhood, by the con-
glomerate, which is the limit of the Chemung group upward. Farther south, near Tioga
point, rocks of the same group occur in the bank from one hundred to two hundred feet above
the river, and some of the sandstone layers are three or four feet thick, and highly siliceous.
I was informed, that on the top of the hill, the conglomerate is quarried for use on some of the
public works below Tioga point. - - -
At the Chemung upper narrows, and at several other localities, there occurs in this group
a stratum of concretionary sandstone of a peculiar character. In a few instances only are
the concretions perfectly formed, but generally have one side imperfect, with a solid nucleus
partially surrounded with concentric laminae, which easily separate from each other; the con-
cavity being often so great as to contain several gallons.
In the valley of Cayuta creek, the group is well exposed in a ravine three miles north of
Factoryville, where fine flagstones could easily be obtained. In the north part of Barton are
CHEMUNG COUNTY, 479
great numbers of loose masses containing the fossils of this group, probably washed down
from the tops of the hills in the vicinity. - -
The shaly rocks of this county are often highly charged with iron pyrites, which on decom-
position stains the shale of an iron rust color. The same gives origin to numerous small
beds of bog ore, which occur in many localities. One of these near Elmira, and another at
Bigflats, furnishes a tolerably pure ore, but in most places it appears as a ferruginous tufa.
On the southern margin of the county, in Southport, there is a small deposit of bog ore, which
apparently owes its origin to the destruction of the conglomerate of the Carboniferous system.
Several beds of shell marl were noticed in this county, and it is probable that further search
will develop more extensive deposits of the kind.
There are several beds of marl near Millport, and the water rising in some of the springs
is so highly impregnated with calcareous matter, that on standing a few hours, a thin deposit
is formed. There is also a deposit of this kind about two miles northeast of Johnson's settle-
ment. In the town of Dix, at the Beaver dam, there is an extensive deposit of marl which
is burned for lime; it is first cut out in large square masses, which cohere on drying, and it
is then placed in the kiln. There is also a similar bed of some extent near the Horseheads:
Shells of Helix, Limnea, Planorbis, Cyclas and others are abundant in the two last named beds.
The topography of this county is very simple. The Chemung river passes through its south
western part, and opens a broad and beautiful valley, bounded by a range of hills, which are
only broken by the lateral streams flowing to the river. The rocks on one side sometimes
approach the river, while on the opposite is an extensive flat or bottom. Here, as elsewhere,
the rocks on both sides of the valley bear evidence of erosion, and show that this river, as
well as other streams, flows in a bed once occupied by rocks like those of the mountain mass.
The eastern boundary of the county is along the valley of Cayuta creek, which has its
origin in the small Cayuta lake, in the north part of the county, and forms a continuous
valley thence to the Chemung river. Wynkoop's and Baldwin’s creek form valleys of less
importance. - ,- - - -
The Chemung valley, extending from the head of Seneca lake to the Chemung river, is the
most prominent feature in the county. It offers the only route by which a canal could have
been constructed, being through its whole extent alluvial, and presenting no remarkable ele-
vations. The ascent from Seneca lake to the summit level of this canal is four hundred and
forty feet in a distance of fifteen miles. -
480 . . GEoLogy of THE FOURTH DISTRICT.
STEUBEN COUNTY.
The general character of the surface of this county is similar to all those of the southern
range. A series of broad irregular hills with low valleys occupy the greater part of the county.
It is also marked by several deep valleys, which present broad alluvial bottoms. The valley
extending south from Crooked lake, the Conhocton, the Canisteo and Tioga, are the principal;
these all unite in one, below Painted-Post, communicating with the Susquehannah.
The rocks of this county are of the Portage and Chemung groups, the line of demarcation
between the two being much better defined than farther east. The lower group appears in all
the deep ravines and along the water courses in the northern part of the county, while the
high grounds are occupied with those of the next group. After leaving the head of Crooked
lake, the rocks of the Portage group are not again seen in the county going southward, although
upon the shore of Seneca lake they extend still farther south, from the greater depth of that
valley. - - -
Along the western shore of Crooked lake, the rocks consist chiefly of sandy and slaty or
argillaceous shale, the former rippled or undulated, showing that each thin layer of the shale
was subjected to the action producing the rippled surfaces, and this action continued uniform
throughout the whole deposit. Alternating with the greenish shale just noticed, is a darker
slaty shale containing fossils. At some localities occur a few thin layers of sandstone, but
these are not abundant until we approach the head of the lake. - -
Four miles below Hammondsport, in a ravine on the bank of the lake, can be seen a con-
cretionary stratum of impure limestone, composed of roundish or irregular masses cemented
together by an argillo-calcareous cement. In other localities, the concretionary forms are not
so distinct; and the whole bears the character of an irregular mass, separated in various
directions by thin seams of shaly matter. So far as examined, this stratum bears a very uni-
form character; it disappears beneath the lake on the east side, one mile below Hammonds-
port. This limestone has been burned, but found too impure for quick lime, though it pos-
sesses some of the characters of hydraulic cement.
At Hammondsport, in the ravine above Mallory's mill, we find about three hundred feet of
rocks exposed, belonging to the Portage group; they are well characterized by the Fucoides
graphica. Few fossils other than fucoids appear through this thickness, though higher in the
ravine are some fossils peculiar to the next group. The mass exposed consists, in the lower
part, principally of shale and thin layers of sandstone, and at a higher point numerous layers
of sandstone from four to ten inches thick. The edges of all the layers exposed, are covered
with crystals of selenite, or crystallized gypsum. About one mile from the mouth of this
ravine, an excavation for coal has been made in the black shale, which alternates with the
sandstone and olive shale. The indications of coal at this point were a few fragments of
vegetables, iron pyrites, and the odor of bitumen arising from the shale; all these were sup-
STEUBEN COUNTY. 481
posed to be unfailing evidences of coal beneath. The work is at present abandoned, until
some new excitement, or reported exhibition of burning gas, shall induce others to engage in
the enterprise. In the shale thrown from this digging I found Cypricardia, Avicula, and several
other fossils. On the east side of the valley, opposite Hammondsport, a similar ravine exposes
the same strata as those just described.
One mile northwest of Bath there is a stratum of very tough argillo-calcareous rock, three
feet thick; the massis filled with fragments of crinoidal columns, presenting surfaces like the
finest birdseye maple. This furnishes some of the finest building and foundation stone, and
should it be of such a quality as to receive a fine polish, it will be a valuable acquisition to
the mineral wealth of the county. A large species of Strophomena and Delthyris occur in the
lower part of the mass. “ --,
The rocks of the Chemung group continue along the valley of the Conhocton to Painted-
Post, and as far up the Tioga as the south line of the State ; the tops of the high hills excepted,
which are capped by the conglomerate in a few places.
The valley of the Canisteo is bounded on both sides by almost unbroken ranges of rocks
of the same group. The same rocks are seen along the valley of Five-mile creek, which
appears to have been formerly a continuation of the Canandaigua lake valley, and the com-
munication between that valley and the Conhocton.
The soil of Steuben, though not as favorable for the production of grain as the northern
counties, is one of the best sections for grazing. From the valleys, the high country seems
broken and uneven; but this is confined to the immediate edges of the hills, for after ascending
to the table land, we find a beautiful undulating surface, which, when farther cultivated and
cleared of forests, will prove one of the best grass-growing regions in the State. These
remarks apply also to Chemung county; and in all the elevated portions of both, the water
is pure and soft. -
The facilities for communication in this county are very great; and when the New-York
and Erie railroad shall be completed, the lateral valleys will afford thoroughfares from all
parts of the county. Uneven as its surface is represented, the valleys of the Conhocton,
Canisteo, Tioga, Five-mile creek, and numerous others, furnish means of establishing smooth
and permanent roads from almost every part of the county. -
The high banks on either side of the valley of the Tioga expose the outcropping edges of the
strata, and numerous small quarries are opened for the extraction of the thin layers of sand-
stone everywhere interstratified with the shale. The hills are capped by thin layers of sand-
stone, with less shale than below, reddish or brownish in color, and highly micaceous. These
upper portions, so far as observed, are less distinctly characterized by fossils.
The rocks, at the south line of the State and near the river level, consist of hard, thick
strata of grey sandstone, a part containing abundance of Strophomena and Delthyris, and
succeeded by a thick concretionary mass. The grey sandstone forms a fine material for
building, and more durable than any other in this part of the country. Farther west, and a
[GEOL. 4th DIST.] 61
482 GEOLOGY OF THE FOURTH DISTRICT.
little south of the county line, a thick mass of concretionary sandstone, with regular strata of
grey sandstone, is seen in the north bank of the Cowanisque creek,
In order to give any definite information regarding the connection of these rocks with those
of known character above, I have found it necessary to extend my examination as far as
Tioga, Pa., seven or eight miles south of the State line. At this place the upper member of
the Chemung group of New-York passes beneath the Old Red sandstone, dipping south at
an angle of from 6° to 89. The Old Red sandstone, a little south of this place, is about four
hundred feet thick, of a brick red color, with beds of softer or shaly rock of the same color,
containing fucoids and bones of fishes. The upper portion, containing the scales of Holopty-
chus, often approaches in character to conglomerate. • ' '
The Old Red sandstone approaches the south line of the county, towards its western limits;
and has been found forming a thin capping upon some of the higher hills in Troupsburgh.
Here, as in other places on its northwestern margin, the rock consists of a thin layer of argil-
laceous sandstone, highly ferruginous in character, and bearing a general resemblance to the
iron ore of the Clinton group. Its decomposition stains the soil a bright red color, and, from
these indications, it has been supposed that valuable beds of ore would be found. It is
necessary to observe, however, that it is extremely doubtful whether this stratum will ever
prove of any importance as an iron ore. In the southern part of the town of Greenwood, the
soil is deeply stained from the destruction of this rock, but I have not found the same in place.
In a section made from Dansville south, through the valley, to the Canisteo, and thence
along Bennett's and Troup's creek to the south line of the State, nearly the same kind of
rocks prevail as previously described, and in the same order of succession; also in the valley
from Patchin's to Loon lake and Howard. - - -
The valley of Loon lake is the continuation of the Hemlock lake and Springwater valleys.
In the neighborhood of the lake, large accumulations of drift rise in rounded hills fifty or
sixty feet above the general level, and skirt the valley on either side; while beyond, the hills
formed by the rocks rise to a much greater elevation. The commencement of the fossilife-
rous strata of the Chemung group is at a little distance north of Loon lake. Few sections
are exposed, and our observations are limited to the loose masses on the surface, and some
shallow ravines where a few feet in thickness of rock are seen.” X-
The country known as Howard Flats, is formed of drift hills and ridges but little elevated
above the general level, being a high and not well defined valley, presenting outlets in various
directions. I could not ascertain the depth of the drift, but the deepest wells do not reach its
termination; and the absence of an impervious stratum in the gravel renders it often difficult
to obtain water in sufficient quantities. - --
* Loon lake is situated in a high valley; the hills on the east and west rise to a considerable height, but on the north and south
there is almost a continuous level, forming an extensive swamp; the lake has no immediate outlet, but its waters supply Neil's
creek, which rises in the swamp, half a mile south. From the north end of the lake an artificial outlet supplies water for mills,
and is continued as far as Patchin's.
STEUBEN COUNTY. 483
In passing from Howard to the Canisteo valley, at Hornellsville, we cross the highest hills
in this part of the county. The rocks consist of portions of the last named group; shaly sand-
stone, shale and siliceous sandstone, all containing fossils, are found along the whole distance.
The northern drift, confined to lower levels, is not seen along the road from Howard to
Canisteo; and the soil is a clayey gravel, formed from the substrata, and not highly water-
worn. In descending into the valley of the Canisteo, we again come upon the northern drift,
which is the soil of the valley, and covers the lower slope of the hills.
Five miles from the Canisteo, on Bennett's creek, there is a thick mass of sandstone, over-
laid by calcareous sandstone, containing abundance of fossils of Strophomena and Delthyris.
The stone is very firm and durable, and easily quarried in blocks of necessary size for build-
ing ; and the part containing fossils is much used as a firestone.
Nine miles from the Canisteo, at Lagrange, in the town of Greenwood, the rocks are seen
both along Bennett's and Rigg's creeks; and at the point of land near their junction are seve-
ral courses of sandstone proper for grindstones. The whole thickness is from eight to ten feet,
and the layers from two to eight inches. In ascending Rigg's creek, these strata disappear
beneath the surface, and are succeeded by greenish shale, with thin layers of silico-calca-
reous rock with fossils. This shale contains iron pyrites, and decomposes rapidly. The
grindstone stratum is visible on the west bank of Bennett's creek, and extends a mile north
to Rock creek, and was also traced up the latter a mile above the junction. Its outcropping
edges are found in the hills farther north ; but the better situations for quarrying are along
the banks of the small streams. The character of the mass is, however, variable ; and its
fitness for grindstones cannot, in all places, be relied on. At the mouth of Rock creek, it is
much harder than at the quarry on Rigg's creek. -
The exposed portions of the strata are greyish-brown, slightly stained with iron, rather
porous and soft, and containing scales of mica. The rock above and below the grindstone
portion is green shale; this, in some places, abounds with fossils, as at Rock creek, while
above, the green shale, fifty feet thick, is not fossiliferous. It contains some thin layers of
sandstone, and is succeeded by a stratum of sandstone about ten feet thick. This latter con-
tains fossils, while the grindstone mass embraces few or none. The upper sandstone is also
more hard and coarse than that below, and well fitted for building, underpinning and ordinary
firestone. This is again succeeded by greenish shale. This place is between four hundred
and five hundred feet above the Canisteo, and fifteen hundred feet above tide water. The
source of Bennett’s creek is about eight hundred feet above the Canisteo, and the surrounding
hills are several hundred feet higher. Four or five miles south of the village of Lagrange, a
sandstone is quarried on the land of Mr. Marshall, and used for hearth-stones, tomb-stones,
etc. Grindstones are obtained in Canisteo, on the land of Mr. Carter; in Woodhull on the
land of William Stroud, esquire, and elsewhere; in Jasper, on the land of Colonel Towsley.
These quarries supply all the surrounding country. They are of great economical importance;
and the occurrence of similar rock in so many different places renders it probable that the
mass is continuous.
61*
484 GEology of THE FOURTH DISTRICT.
On the land of Mr. Davis, at Lagrange, a salt spring rises in the green shale; the water
is turbid, and emits bubbles of carburetted hydrogen gas. Several years since, salt was made
at this place, and previously by the Indians. There are, however, no inducements for dig-
ging; for, so far as we know, no salt springs of importance are found in this rock, and it is
probably only such a one as might occur in any marine formation. -
There are numerous beds of lake marl and tufa in this county, some of which are im-
portant as furnishing lime. Two miles northeast of Arkport, there is a bed of this kind which
furnishes a considerable quantity of lime. There is another similar one south of the village,
from which lime was formerly burned. In the town of Troupsburgh there is a bed of this
marl, but it has not yet attracted notice. There is an extensive deposit on the Canesaraga
south of Dansville, from which lime is burned. The summit level between this creek and
the Canisteo presents an extensive muck swamp, and some beds of marl, but their extent
has not been ascertained.
ALLEGANY COUNTY.
The general elevation of this county is higher than Steuben and Chemung, while the rocks
are the same; a difference produced both by a greater thickness of the mass, and a dip to the
east or southeast. -
The northern part of the county is occupied by the Portage rocks; the lower portion of
these rocks, however, is rarely visible, except in deep ravines or water courses. The upper
part of this group forms the cascades and deep escarpments along the line of their northern
outcrop, in many places extending beyond the limits of the county into Livingston and Gene-
see. At the falls on the Canaseraga, in the town of Burns, the Portage rocks are much ex-
posed; but it is at Portage, as has been before described, that they are fully developed, and
may be seen in perpendicular cliffs from two hundred to three hundred and fifty feet high.
The same rocks are traced along the Genesee valley for several miles, when they are suc-
ceeded by the olive shaly sandstone and black micaceous shale, which occupy a part of the
towns of Eagle, Pike, Centreville, Burns and Portage. The thin layers of sandstone inter-
stratified with the black shale, and also those usually succeeding it, are quarried on the Wis-
coy, a mile west of Pike centre, near Pike hollow, and at many other places along the out-
crop and in the ravines and valley sides. - -
The upper part of the Portage group consists of a mass of slightly argillaceous sandstone,
compact and fine-grained, from one hundred and fifty to two hundred feet thick, in some
ALLEGANY COUNTY. 485
places containing pyrites which stains the rock an iron-rust color. This sandstone is quarried
in blocks from one to three feet thick, and of any required size; it breaks easily when first
quarried, and will scarcely stand the vicissitudes of climate. *
The tunnel at Portage is excavated in this rock, and the bank of the river above exposes
it for one hundred and fifty feet, where it is cut for the passage of the canal; and again it
appears at the north end of the bridge at Portageville. At these places large quantities of the
rock have been quarried and dressed in blocks of various sizes for use on the locks, aqueducts,
etc. of the Genesee Valley canal. At two or three other places within three miles south from
Portage, the same rock is quarried in the shallow ravines along the valley of the Genesee
river. & - - - -
Succeeding the black micaceous shale, are the sandstones and shales constituting the Che-
mung group, which is every where visible in the ravines and banks of streams. Its northern
limit extends through the south part of the towns of Centreville, Hume, Grove and Burns,
and its characters are better developed in the next range of towns. In this county, more par-
ticularly along the Genesee river and west, the group differs in lithological characters, and
consequently in some degree in fossils, from the same rocks in Steuben and Chemung; the
latter containing more sandstone, and the shale having an admixture of siliceous matter, that
renders the whole harsh to the touch. In the ravines along the Genesee river, a much larger
portion is pure aluminous shale, of a deep green or bluish-green color; in this, at intervals,
there are courses of nearly pure sandstone; sometimes a single layer of a few inches, at other
times several, forming a mass of four to ten feet thick.
A very good exhibition of this group, and better than is elsewhere seen, in Allegany county,
is on the Caneadea, from Rushford, near M'Call's mills, to the mouth of the creek. The
rocks consist of numerous alternations of shale and sandstone, the latter, often in layers of two
or three inches, and other thicker ones, which are quarried for lockstones, building stones, and
grindstones. One stratum of this sandstone, containing several courses of variable thickness,
affords a good material for grindstones, for which it is quarried on the land of Mr. Bannister.
I did not learn the amount annually taken from this quarry, but judgingfrom the numerous and
distant points where the “Rushford grindstones” are sold, it is greater than any other in the
district. - - - -
Rocks similar to the last, but none of the same strata, are seen in Black creek, Crawford’s
creek and White creek. In the banks of Black creek, at Rockville, some thick masses of
sandstone alternate with green shale, which is slightly calcareous and contains abundance of
fossils. Two of the sandstone strata are about six feet thick each, and divided into courses of
from two to three feet. Similar sandstone is quarried half a mile southwest, on the line of
the canal; it contains fossils of Atrypa and Deltyris ; and a mile and a half south, and sixty
feet higher than the last, a sandstone is exposed on a bank of a small stream. The layers are
thin, but extremely siliceous and durable. - -
The rocks at Rockville are all highly bituminous, the sandstone so much so that it scents the
clothes of the workmen; and the water of the springs, though clear, has the taste of bitumen.
486 - GEOLOGY OF THE FOURTH DISTRICT.
Southeast of Rockville, on White creek, we find a greenish shale, with a concretionary
sandstone, which in some places becomes a conglomerate in the upper part of the layers.
When not concretionary, it is fit for grindstones. Sandstone appears in nearly all the ravines
in this neighborhood. - -
The bed of the Genesee river, at the Transit bridge, is in a mass of very fossiliferous sand-
stone, some portions of which are slightly conglomerated. r -
At Hull's mills, near Angelica, the rocks are exposed in the bank of the creek, for fifty
feet or more in height. They consist principally of shale, which contains the fossils common
to the Chemung group, and among others, the large Pecten-like Avicula. The lower portion
of the mass is a hard grey sandstone, containing in some parts, great numbers of fossils, among
which Delthyris and Strophomena are most abundant. This sandstone has been quarried for
building; it is durable, and presents a very good appearance. -
About a mile and a half south of Angelica, sandstone has been quarried, though the greater
portion of the rock exposed is shale. The sandstone has been used in the construction of a
mill near the quarry; though, when first quarried, it is extremely friable, and scarcely coheres.
Like most sandstones of this region, it contains a large proportion of moisture. ... "
The sandstone along Van Campen's creek was quarried by Judge Church, and used in
building more than thirty years since ; it still remains firm, though somewhat iron-stained
from the decomposition of pyrites. -
At Philipsburgh, two and a half miles south of Hobbieville, we find a change in the rocks,
which is indicated by their fossils more than their lithological character. Green shale is the
predominating portion of the mass ; with some thin strata of sandstone, it occupies the bed
of the river for an eighth of a mile, and, together with the vertical bank, presents a thickness
of forty feet or more. Above Philipsburgh, on the Genesee, rocks similar in character occur
in several places in the bed and bank of the river. At Wandermark's creek, five miles from
Philipsburgh, we find the green shale, not so highly fossiliferous, and with it thin courses of
coarse-grained sandstone, containing abundance of a large species of Delthyris. This fossil
occurs in a rock of similar texture in many places of the same elevation, and may be found to
constitute a definite point, or to mark the termination of some group ; certain it is that along
this line we find scarcely any fossiliferous rocks above it.
The next place south of Vandermark's creek, where rocks are seen, is on Dike creek, near
Wellsville, at an elevation of sixty or seventy feet above the Genesee, and between fifteen
hundred and sixteen hundred feet above tide water. The rock at this place consists principally
of grey sandstone, embracing a brick red or brownish mass six or eight inches thick. This is
composed of sand, or rounded particles of quartz, with much argillaceous matter, splitting into
laminae half an inch or an inch in thickness, and is so highly impregnated with iron that it
stains the hands nearly as much as the oolitic ore of Wayne county, but is not, like that,
unctuous to the touch. It is considered by the inhabitants as a stratum of iron ore; but its
specific gravity proves the proportion of metal to be too small ever to repay working. Single
joints of crinoidea occur in this and the grey rock below. On close inspection, the materials
ALLEGANY COUNTY. 487
of this mass appear to have been subjected to much wearing action, and many specimens
exhibited numerous fragments of bones, apparently belonging to fish, and similar to those found
in the red sandstone on the Tioga. - - .
This rock, examined here and several miles south, is succeeded by a mass consisting of green-
ish grey sandstone, often appearing as if deposited from opposing currents, and in all respects
resembling that succeeding the red sandstone on the Tioga. In examinations further south, I
have not been able to discover the red sandstone, neither along the Allegany and its tributa-
ries; and I am informed by Mr. Horsford, that he saw nothing of it in his journey down that
river as far as Warren, Pa., which brings us to the northern limits of the coal. -
The strata above the red rock at Wellsville, those on the Shenunda creek and towards the
Pennsylvania line, contain no fossils. The mass greatly resembles that above the red sand-
stone elsewhere ; and the great elevation of the points examined, considered with the differ-
ence in altitude between this and the Tioga, may lead us to expect these rocks in place as far
north. This sandstone is elsewhere associated with the conglomerate, occasional fragments
and boulders of which are found in the elevated lands of Steuben, and the eastern part of
Allegany. * -
About three or four miles south of Wellsville, the side hill and valley east of the Genesee are
strewed with masses of the same, consisting of small and large pebbles of white quatrz with
coarse sand. From the great numbers of fragments, we would infer the rock to be in place
nearby, and in a former section this position was given to the conglomerate; and though from
careful investigation I am not able to find it in this vicinity, the position is undoubtedly correct;
for it appears on the hills west of the Genesee, in Scio, and several other points. Its thick-
ness, however, is not so great as I had supposed from its extending over so great a surface.
In Scio, it is found on the high grounds near the sources of some small streams flowing into
the Allegany and Genesee. For the most part the rock appears in large detached masses,
being divided by the joints into rhombic blocks; one of these measured forty-four by sixty
feet, and fifteen feet in thickness. Approaching the rock in place, the masses are larger and
closer together, being but slightly moved out of place, and the spaces between them diminish-
ing from a distance of five or six feet to fissures of a few inches. The sides of the blocks
appear water-worn, or deeply weathered; and the upper surfaces slope in the direction of the
hill, probably from the removal of the rock beneath. The mass seems to have contracted on
desication ; and the joints, since enlarged by the percolation of water from above, form, within
the rock, passages of greater or less extent, communicating with each other. This mass is
composed of pebbles of crystalline quartz, white or rose-colored, from one to two inches in
diameter, and generally elongated or egg-shaped. In the early settlement of the country, this
rock was used for mill stones; but in much the greater part the pebbles are too large, and it
is too friable for this purpose: its use is now superseded. '.
Previous to visiting this place, I was informed that a bed of coal two feet thick had been
found beneath this conglomerate, and it was represented as having been used in the blacksmith's
forges. On further inquiry, I could not learn that such a bed was known ; the only person who
488 GEOLOGY OF THE FOURTH DISTRICT.
could give any information of its existence, had seen small pieces not more than one-half inch
in diameter. - -
This is the only rock seen on the surface, between Wellsville on the Genesee, and Bolivar.
In the town of Genesee, about three miles north of the Pennsylvania line, and near the
centre of that town, the conglomerate, essentially the same as at Scio, occurs on the highest
hills. -
On the Little Genesee, a few rods north of the Pennsylvania line, sandstone and shale with
fossils appear in place; this is at nearly the level of the stream, two or three hundred feet
below the conglomerate. I saw, also, some detached masses, resembling the red rock at
Wellsville, and a reddish soil which may be caused by the outcrop and disintegration of the
same stratum. Along the southern line of the county the rocks are interrupted by the valley
of the Oswaya creek, and thus we have no means of tracing their continuation or immediate
connection with those of Pennsylvania. ,' Y
At several places in the western part of this county, as at Cuba, we find rocks of shale and
sandstone similar to those already described, and quarries are opened to some extent.
West of the village of Cuba is another more extensive quarry on the land of Judge Cham-
berlayne; this affords sandstone in thicker masses, and better fitted for building than the
others. - -
Between Cuba and Friendship, rocks scarcely appear in place, though they are not far
beneath the surface. In most of the high grounds of the southern counties the soil is shallow,
the substratum being but a few feet beneath it, - - -
*
CATTARAUGUS COUNTY.”
The general surface of Cattaraugus county maintains about the same elevation as Allegany;
the Genesee in the former, and the Allegany river in the latter, also take their rise at about
the same altitude, and continue their course with nearly the same descent, though flowing in
nearly opposite directions. Although this county is crossed by numerous streams of conside-
rable size, still there are few situations where a good view of the rocks can be obtained. The
valley of Ischua creek, which extends nearly across the county from north to south on its
eastern side, exposes the strata only in a few places. The Cattaraugus creek pursues its
course for the whole distance, in the outcrop of the strata, consequently developing but one or
two rocks. -
The rocks of this county are a continuation of the same groups noticed in Allegany county.
The Portage group forms the northern boundary of the county, and is exposed along the
* The details of this county are mostly extracted from Mr. E. N. HoRSFORD's Report. Annual Report of 1840.
CATTARAUGUS COUNTY. *: 489
Cattaraugus creek. This is succeeded by the same shales and sandstones as before noticed
in Allegany. There appears, however, a general diminution in thickness of all the masses
to the westward; and many which in Allegany are of great thickness, appear here much
diminished. 3. r
Notwithstanding that the rocks are exposed at few places, still, from the great elevation of
the country, and the thinness of drift or alluvium, they are found at moderate depths below
the surface. - - - -
This county is among those of the Fourth District distinguished for their deep and extended
valleys, and their ranges of elevated hills. The proportion of uneven surface throughout, but
particularly in the southern part, is somewhat greater than in either of the counties of the
same range, directly east.
The general direction of these valleys is the same as that of the large valleys farther east—
from north to south. Toward their northern extremes, the beds of most of them expand gra-
dually into plains of considerable width, limited by acclivities of gentle ascent on either side ;
while some branch into smaller and more irregular valleys. They become, also, more and
more shallow, to the north. But in their continuation southward, their depth constantly
increases, the hills become more elevated, and the declivities more precipitous. The summit
of some of the highest points of land cannot be less than eight hundred feet above the low
grounds of the surrounding valleys.
Along the northern border of the county, there is spread out a body of alluvium totally
distinct in character from that prevailing in the southern portions; and the difference between
the two is manifest, as well in the vegetation with which they are clothed, as in the materials
of which they are composed. The ravines and gorges of the one have fewer evergreens, and
of these the hemlock is the most abundant, while the valleys of the Allegany and its tributa-
ries are distinguished for their forests of pine. -
No region of this State, and probably none of any other in the Union, was originally
covered with an equal amount of valuable timber. Some of the trees have measured two
hundred and thirty feet in height, and five of them have been known to furnish an hundred
“lumberman’s” logs. Shingles and boards for the supply of the whole western world, from
one extreme of the Union, Louisiana, quite half way to the other, have been manufactured
in the shingle shanties and saw-mills upon the Allegany and its tributaries.
The lands of the valleys, and indeed of the entire county, with the exception of here and
there limited areas, are susceptible of cultivation. The only swamps worthy of notice are
the Conewango and the large one northeast of Waverly. Clay underlies a considerable pro-
portion of these, and, we were informed, the whole of the former. Deep ditchings would
reclaim, large portions, if not the whole of both, and will, without doubt, as the country
around becomes more settled, be adopted. Hitherto, the lands having upon them groves of
timber, and contiguous to mill-sites, have been more valued for the lumber they furnished,
than for the crops they might have been made to produce. The occupation of the lumber-
man, however, must soon be much less productive than at present, and ultimately give way
[GEoL. 4th Dist.] 62
490 GEOLOGY OF THE FOURTH DISTRICT.
to the duties of the husbandman. When it shall, and when the lands of the valleys enjoy the
cultivation given to the flats of the Genesee and Mohawk, there are portions of Cattaraugus
that will present fine farms and yield valuable incomes.
The beds of clay, marl, tufa, bog-iron and manganese, and the swamps are mostly in the
depressions of the alluvium. -
The surface soil is a yellowish loam, chiefly composed of disintegrated sandstone and shale.
It has been washed down from the hill sides and cliffs, by rains and the melting of snows, and
emptied into the streams which, in their overflowings, spread it out upon the low lands of the
valleys. It is the principal soil of the Allegany valley, and of the flats along the Cattaraugus
creek. ta - -
Clay, in shallow beds, is found more or less in the valleys, but to no extent was it seen
upon the higher lands. That of the Conewango is by far the largest seen. It is observed at
Randolph in several places, and probably underlies a great portion of the immense lowlands
and swamps. It is seen a mile west of Waverly in strata, and alternating with gravel and
sand in an alluvial hill directly south of Waverly village. It is found about a mile south of
New-Albion, a hundred yards from the mouth of a tributary to the stream, along which the
road passes.
In the towns of Great-Valley and Little-Valley, the “sags” or depressions in which the
clay is formed, contain more or less extensive bodies of peat. The largest is upon the land
of Mr. Sweetland. About ten acres are spread over by the bog; and the depth of peat varies
from a foot or two near the margin, to more than twelve towards the centre. As a manure,
and as a substitute for coal and wood, this bed in particular, and the smaller ones in propor-
tion to their extent, must become of value. For the improvement of lands, the peat may be
appropriated immediately and with great profit on most farms.
The occurrence of peat is generally indicated by the growth of dwarfish evergreens, and
rank swamp herbage, and by the elasticity of the crust which supports them. -
There is an extensive bed of marl about two miles from Lodi, upon a small branch of the
Cattaraugus creek. It lies southeast from the village, and about a quarter of a mile from the
mouth of the branch. A kiln has been in operation a number of years, and several thousand
bushels are burned annually.
In the east part of Otto, upon the land of Mr. Sias, a bed of marl covers between three and
four acres, and is from a few inches to four feet deep. About one thousand bushels have
been burned annually. With this marl there are no foreign substances, except now and then
a little vegetable mould, which all disappears in the process of burning. Estimating the area
at three and a half acres, and the average depth at one foot, we have 122,500 bushels, a
quantity that will supply the demand, should it increase to three thousand bushels annually,
for forty years to come.
A small bed of tufa furnished a few kilns with lime in Dutch hollow, in the town of Ash-
ford, but is now nearly exhausted. A number of small beds have been found near the resi-
dence of Mr. Sias, and we were informed that a bed of some extent had been discovered in
CATTARAUGUS COUNTY. 491
New-Albion. Near the mouth of the Canaseraulie a bed has been found, and another near
Zoar, with several intermediate ones, but all are small and have not been worked to any extent.
Upon the land of Mr. Hancock, in Freedom, a bed covering a considerable portion of three
acres, has been opened. The better portions of it are nearly exhausted, though much yet
remains that may be advantageously used for agricultural purposes. From 3000 to 6000
bushels have been burned annually for the last twelve years. There is another large one in
the north part of Freedom, owned by Mr. Sherman. Four miles southeast of Randolph, on
the land of Judge Leavenworth, a small bed has been found. -
Taking the whole together, there are in the county materials, of marl and tufa, enough to
furnish immediately 300,000 bushels of lime. -
Beds of bog iron ore are found in many little swamps and lowlands in different parts of the
county. Across the river from Olean, masses containing several cubic feet have been exca-
vated. ^- -
The earthy oaſide of manganese or wad, was found in different parts of the Conewango and
Little valleys. More was seen upon the land of Mr. Bush, in Randolph, than in any other
place. It is accumulated in nodules, in some places, from the size of a shot, up to that of a
walnut. In other places, it is seen adhering to fragments of sandstone, scattered throughout
the soil. It has not yet been found in quantities sufficient to be of value.
Near Lodi, nodules of iron pyrites are found in considerable quantities, in the upper por-
tions of the gravel alluvium, underlying the loam of the valley.
Trappean, hornblendic, gneissoid, granitic and sienitic, and some other boulders, are the
representatives from more northern latitudes. One boulder of hypersthene was seen at the
sulphur springs near Randolph. Two boulders of iron ore, resembling the specular ore of
St. Lawrence county, were found on the south branch of the Cattaraugus, near Little's mills.
One weighs thirteen pounds. Both have been procured for the State Collection.
Salt springs or licks are occasionally found. Several near Rutledge attracted attention in
the early settlement of the town, from the numbers of deer who came to “lick” about them.
Near one of these a shaft was sunk, in the hope that lower down the strength of the brine
would be found greater. The proportion of salt was, we are informed, about a teaspoonful
to a pail of water. . . " -
The Oil spring, of Freedom, is, in many respects, like that of Cuba in Allegany county.
Its diameter is somewhat less, and the quantity of oil which in a given time rises to the sur-
face is, in proportion to its extent, the same. - -
Carburetted hydrogen is emitted at this spring, in small quantities. It is observed to
escape from almost all waters, either stagnant or running, in the county. It is seen bubbling
up through the waters of most large springs. The only place where the quantity is sufficient
to maintain a constant flame, is at the mouth of a small stream coming in to the Cattaraugus,
against the Missionary house, about five miles above Lagrange.
Sulphur springs are occasionally met with. One upon the land of Judge Leavenworth,
near Randolph, is pretty strongly impregnated.
62*
492 GEOLOGY OF THE FOURTH DISTRICT.
The conglomerate is the highest rock in the series that has yet been observed in the State.
Immense blocks of it are found at Chipmuck ripple on the Allegany river, and near Judge
Wright's, southeast of Ellicottville; also between Napoli and Little-valley, on the James-
town and Ellicottville stage road, near Judge Leavenworth's, and at numerous other loca-
lities. But the places where it is seen in situ are comparatively few, and only upon the
very highest points of land. One, five miles south of Olean; two between Great-valley and
Little-valley, and several south of the Allegany, comprise all in this county concerning which
information was obtained. The locality best known is about seven miles south of Ellicottville,
and one and a half west of Great-valley post-office. It is known as the Rock city. It is
approached along a ridge extending from the base to the top of the hill, of gradual ascent, and
terminating at an elevation of not less than six hundred feet. Other hills, upon the opposite
side of the valley, and of less altitude, were determined by Col. Hawley to be above six hun-
dred feet in height. - .
From the abundance of timber in Cattaraugus, little need of good building stone has
hitherto been felt, and, consequently, little exploration has been made for valuable quarries.
Of those opened in different parts of the county, the greater part will be found noticed in
the list which follows. -
The quarries at Olean contain micaceous sandstone, and an olive shale, which is concre-
tionary. The stone at the lower quarry are coarse; while at the one some fifty feet above,
they are of a finer grain. The underpinnings and cellar walls of many buildings in Olean
have been obtained from them. A quarry owned by Mr. Pratt, in a small alluvial hill, a hun-
dred rods down the river from the quarries above noticed, is nearly exhausted. In a ravine
which is entered just south of Pratt's quarry, there are found masses of a coarse sandstone,
like that alternating with the conglomerate which is seen a few miles farther south. These
masses are strewn along the ravine its entire length. The same rock occurs in several places
along the Allegany, in huge fragments, and is seen to be of the most durable character, from
the angular form of the masses, notwithstanding their long exposure to the action of the cur-
rent. From examinations made in Pennsylvania, its true place is ascertained to be in the
lower part of the conglomerate. - .
Nine miles below Olean, sandstone, slightly concretionary, has been quarried for the filling
up of dams and other purposes. -
The Ischua stone quarries, lying almost wholly in the town of Machias, contain stone with
which there are none other in the county to be compared, either for beauty when dressed, for
the facility of quarrying, or for durability. They are a coarse sandstone, disposed in massive
and in thin layers, of such thickness, that blocks for every desirable purpose, from heavy
columns to thin flagging stone, may be easily procured. Butler's quarries, three miles north
of Franklinville, have been most extensively worked. The foundation walls of Irvine Hall,
Ellicottville, were here procured. The quarries are in the visible outcrop, which extends for
a considerable distance. -
CHAUTAUQUE COUNTY. 493.
All the important quarries in this county were enumerated in the Annual Report of 1840,
and, therefore, need not be repeated in this place. They afford but little variety; and, from
what is known of the same group of rocks here and elsewhere, no other economical or valua
ble products are to be expected from these rocks than the ordinary quarry stones.
CHAUTAU QUE COUNTY.
The general face of the country in this county resembles that of all the southern counties
in the district. It differs in some degree, however, in its soil, which is of a loamy character
in a greater proportion than many others. The hills, although of the same nature, are less
elevated, either from the general elevation having originally been less, or that the abrading
action has been more effective. The latter may perhaps be the cause, as the proportion of
hard materials is less than farther east, and there is also evidence that the rocks all grow
thinner on going westward, and in Ohio the highest rocks of Chautauque county are but a
few hundred feet above Lake Erie. -
It has been ascertained from surveys, that the highest parts of this county do not attain so
great an elevation, by two hundred feet, as some parts of Cattaraugus and Allegany. The
broad valley of the Conewango on the east side bounds the county by a depression of five
hundred to eight hundred feet lower than the high hills; while on the north, the deep gorge
of the Cattaraugus creek is even lower than that of Conewango. On the northwest side we
descend, in the distance of five to eight miles, from an elevation of about two thousand feet
above tide water, to Lake Erie, (which is five hundred and sixty feet above the sea,) nearly all
the descent being in the first three or four miles. This is a remarkable feature in Chautau-
que county, and one which can only be accounted for by supposing the abrasion and removal
of the materials once filling this space. - -
Another remarkable feature in Chautauque county, is the existence of the lake of the same
name, the northern extremity of which is only eight miles distant from Lake Erie, and yet
empties its waters by the Conewango, Allegany, Ohio and Mississippi into the Atlantic. This
lake is sixteen miles long and twelve hundred and ninety-one feet above tide water, and seven
hundred and twenty-six feet above Lake Erie. It is a beautiful sheet of water, bounded on
its eastern side by gravelly sloping banks, and on the west by more level and in some places
marshy shores. The channels of the streams flowing into the Allegany are all, more than
twelve hundred feet above tide; the valleys and hills range at all points between this height
and two thousand feet. . • * * * º
To superficial observation there are few rocks to be seen in Chautauque county, but exami-
nations made along the deep ravines prove the existence of all the great masses further east,
and from the destruction of which the soil of the county is mostly produced. 3
Along the lake shore, from near Cattaraugus creek to the State line, we find the banks are
494 GEOLOGY OF THE FOURTH DRSTRICT.
perpendicular bluffs from ten to one hundred feet in height. Green shale alternates with the
thicker courses of black, and beyond this the black shale increases in proportion as far as
Portland harbor. Both green and black shale contain septaria, and more rarely, thin sandy
layers, which are so numerous in the Portage group, constituting the flagstones further east.
From Portland harbor to the State line we have similar slaty and crumbling shales, alternating
with thick and thin courses of sandstone, all possessing a similar general character. Arriving
at the State line, we are able to trace the same group in the deep ravines for two or three
hundred feet higher before there is any marked change. Throughout the whole extent there
are scarcely any fossils except fueoids, and these abound wherever the thin sandy layers
CCCUlſ.
All the northern part of the county below the elevation of fourteen hundred feet above tide
water, or about eight hundred and forty feet above Lake Erie, is underlaid by the shale and
thin sandstone of the group above mentioned. These rocks are distinguished from those
above by the almost entire absence of all fossils except fucoids, as well as the greater pre-
dominance of shale. In the southern part of the county the rocks of this group are not seen,
having passed below the level of the lowest valleys. º
All the southern part, as well as the higher portions of the northern part, are occupied by
the Chemung group, readily known by the great number of shells of the genera Strophomena,
Orthis, Delthyris, Avicula, &c. which characterize it every where. In this group the pro-
portion of sand increases over that below, and in its upper part the larger proportion is sand-
stone. -
The rocks of this group can be seen to great advantage in the Chautauque creek, six miles
above Westfield, and in the outlet of Chautauque lake below Jamestown. They can also be
examined to some extent above Rice's mill on the Twenty-mile creek, and in many of the
ravines along the Conewango and Cassadaga valleys. The strata are no where seen except
in ravines or the banks of streams. * , -
The extreme southern part of the county is comparatively low, rising to less elevation than
the middle portions. - - -
Many of the hills are capped with conglomerate, which is the highest rock in the county.
From the portions remaining, the rock appears to have been originally of variable thickness;
in some places not more than five or six feet, and in others fifty or sixty feet. Where the rock
is free from pebbles, it is known by being more friable than any of the sandstones below; and
also by the lines of deposition being at varying angles, as if acted upon by currents from diffe-
rent directions. In such cases it forms a good building or underpinning stone, easily dressed,
and readily obtained in blocks of large dimensions. It is, in fact, almost the only stone in the
southern part of the county which can be obtained more than a few inches in thickness.
The principal places where it is quarried are, upon the top of a hill about two miles from
Ashville; another quarry four miles north of Panama, and again one mile northwest of this.
From these places, considerable quantities of the rock have been taken. It is associated with
a few inches of the coarse conglomerate. -
On the north side of Chautauque lake, it occurs on the land of Mr. Young; also on the
CHAUTAUQUE COUNTY. - 495
land of Mr Barnard and Mr. Preston, passing from Ellington centre to Cassadaga creek; and
again farther north, on the land of Mr. Strong, three miles north of Ellery centre. In all
these places it is found only in loose blocks scattered thickly over the surface for a small
extent, and evidently the remains of a once continuous stratum.
At Panama the conglomerate occurs upon both sides of the stream between the upper and
lower village, and follows the eastern slope of a hill for more than half a mile. Where I
measured it upon the stream, it was about sixty feet thick. It lies in huge masses sixty or
seventy feet long by twenty or forty wide and thick, with deep fissures between. Sometimes
the masses are so arranged that these fissures form caverns; and one place I was shown, is so
excluded from sunlight that snow and ice remain during the summer. These masses dimi-
nish in size and frequency towards the south, and soon disappear. -
Four miles northwest of Panama, on the land of Mr. Field, the conglomerate and sand-
stone are found covering the ground to considerable depth. The whole is composed of frag-
ments, most of them small, which are piled irregularly one above the other, as if rolled down
from a higher eminence. The situation is at the foot of a hill upon the western side. Several
miles west of this place, in Clymer, there is a locality of this sandstone, which has formerly
been quarried for grindstones, and also for other purposes. -
About three miles southeast of Panama, on the east side of the valley of the Little Broken
Straw, the conglomerate is found on the land of Mr. Lloyd. Still further east, on lot 13,
land of Mr. Vosburgh, the sandstone occupies the surface of two or three acres, outcropping
on the northern and eastern sides of the hill. In digging a well near the summit of the hill,
the same rock was found. It was covered with a layer of “fine beach sand;” the rock be-
neath was fractured, and the surface worn and smooth. -
It is nearly impossible to indicate every point where this rock may be found; those men-
tioned have been personally examined; other places probably occur, but the hills are frequently
covered with forests and without road. The only remaining places to be noticed, are two hills
in the southeast corner of the county, on either side of Case Run, which I visited on my way
south to Warren. The mass, consisting mainly of sandstone, with little conglomerate, lies
scattered over the sides of the hills and upon the tops, in huge blocks, the thickest noticed be.
ing about thirty feet. This locality is on a range of elevated ground which extends southward
between the Allegany river and Conewango creek; the conglomerate and grey sandstone ac-
companying it, are seen, with some interruptions, nearly the whole distance to the point where
these two streams meet. Six miles south of the State line, there is a thin bed of coal, appa-
rently resting upon the conglomerate. - - -
The soil of Chautauque is principally of two characters. That resulting from the decom-
position of the rocks in place, is a clay loam mixed with angular and unworn fragments of
the harder portions of the rocks, and known as the “flat gravel.” This occupies all the hills
and a large portion of the higher ground.
The materials of this soil are coarser as we descend beneath the surface, and below are
frequently composed of large angular masses, closely impacted together, and forming a mass
of variable thickness, lying upon the surface of the rock beneath. Where in such cases the
496 GEOLOGY OF THE FOURTH IDFSTRICT.
surface of the rock below is level, it is scratched and worn smooth, evidently from the mates
rials having been moved along its surface. In one place near Portland harbor, in opening a
quarry, a considerable quantity of this kind of material was removed; the larger masses fit
for rough walls were left, and the finer thrown into the lake; the quantity thus reserved was
sufficient to have covered the whole surface, when packed closely, to the depth of four feet,
though the original depth of the whole was only five or six feet. Numerous similar instances
appear in the bluffs of gravel along the lake; the moving force seems to have torn up the sur-
face layers, and to have pressed them onward, accumulating in power and quantity, liſting the
strata for great distances, bending and breaking the uplifted edges, and leaving them in all
manner of contortions, with rounded gravel above and below. In some instances the gravel
is forced under the uplifted edge of a stratum to the distance of many feet. -
The valleys are covered with a soil consisting of fine loam and gravel of rounded ma-
terials, which has been derived from more northern rocks. Many of the lower valleys have
evidently been overflowed with quiet water, from which the fine loamy deposits have been
made. - - - - **
The small lakes, Bear lake, Cassadaga lake and Mud lake, have once been much more ex-
tensive; and by successive drainage, they have left marks of their subsidence along the sloping
hills around them. The valleys of the Cassadaga and Conewango creeks have evidently been
extensive lakes, as would appear both from the nature of the materials in the bottom of these
valleys, and from the evidences along the elevated grounds bordering them, as also from the
narrow outlets worn through rocky strata. -
In the valley of the Chautauque lake, we find satisfactory evidence of its former greater
elevation in ridges or terraces of gravel and sand; these are particularly well defined upon the
north side. On examinations about the outlet, the cause of this greater elevation is found to
have been the obstruction of its former outlet, which was nearly in an easterly direction from
the Cassadaga ; whereas now, by the accumulation of large deposits of gravel, it is turned in
a southerly direction, and only joins the Cassadaga valley by a channel excavated through the
solid rock. This direction is seen very clearly by examining its course on a map, and the .
effects of the wearing action upon the rocks are still visible at Dexterville below Jamestown.
At the time the original outlet was obstructed, the waters of the lake must have been raised
to more than thirty feet above the present level, overflowing for a great distance the low
valleys on its western side and its northern extremity, and which exhibit clearly the evidence
of such condition from the almost level deposits of fine alluvium which cover them.
Deposits of marl are less numerous in Chautauque county than in the counties farther east.
The largest deposit of this kind is in Cassadaga lake and the marshes which nearly divide it
into two portions. This marl has been used for several years for burning into lime, of which
2000 bushels are annually made. There is a bed of marl and tufa at the southern extremity
of Chautauque lake, near Dexterville.
In many places, recourse is had to large boulders and transported fragments of limestone for
burning into lime. One of these masses, found near Forrestville, yielded one hundred and fifty
CHAUTAUQUE COUNTY. - 497
barrels of lime. A few miles southeast of Fredonia, a large mass of the water limestone was
found, which burned into quicklime of a dark color. This gave rise to the belief of the exis-
tence of the same rock in place in the neighborhood, but it will not be found south of the lime-
stone terrace in Erie county. - - - - -
In the southwest corner of the town of Clymer, and within a few rods of the Pennsylvania
line, Mr. Beardsley has opened a quarry which affords good grindstones. The rock is of
great extent, and can be easily quarried for all the supply required. It is of the same stratum
as that quarried in Freedom in Cattaraugus county, and in Rushford in Allegany county. The
same is also to be seen in the western bank of the Little Broken Straw, below Panama. It is
here characterized by a species of fucoid, found also at Freedom and Rushford.
Few of the layers are thick enough to afford good building stone, though there are some
quarries of this kind in the Portage group. The principal which I have seen in Chatauque
county, are near Forrestville, and about four miles from Fredonia, on the line of the railroad.
The rocks from the two quarries near the railroad have been used in constructing the arches
over the streams for the passage of the road, and in the public works at the harbor of Dun-
kirk. s
Quarries have been opened at Shumla on the Canadawa creek, and at Laona on the same
stream. The mass at Laona is about five feet thick; the upper three feet often forming but
a single course, thus affording blocks of large dimensions. It is highly bituminous, and petro-
leum is seen on the water which rises from the earth in the vicinity of the rock. Going south-
ward this mass becomes much thinner, and at Westfield there is no appearance of it, except
in a layer of about one foot thickness, and considerably changed in character. It appears to
have been deposited in a depression of the strata below, which causes it to grow thinner on
either side. . - - -
About three miles south of Fredonia, there is a quarry of shale and sandstone from which
some blocks have been obtained of about a foot in thickness; these are succeeded by shale
and thin layers of sandstone. - .
The rocks occupying the high grounds of the southern part of Erie and the northern part
of Chautauque afford excellent flagging stones, some of them of large dimensions. Those
about Boston, in Erie county, are commonly eight to ten feet long and ten to twelve broad,
and sometimes are obtained of twice these dimensions. Near Westfield, in Chatauque county,
these flagging stones are obtained of very large dimensions, often fifteen or twenty feet in
length, with a width of ten or twelve feet. The surfaces of these are rippled in large waves.
The same courses of rock are very extensive, and everywhere furnish this material.
The localities enumerated under the head of Conglomerate, afford excellent building stone
of any required dimensions. From some of these places large blocks of stone for pillars,
etc. have been taken to Mayville, Dunkirk and Buffalo.
Carburetted hydrogen gas is every where common in the higher rocks of New-York, and
in Chautauque county is unusually abundant. In many places the escape of this gas is ac-
companied with petroleum, which forms a pellicle upon the surface of the water, indicating
[GEoL. 4th DIST.] 63
498 - GEOLOGY OF THE FOURTH DISTRICT,
the escape of the gas; in other places the gas rises alone, and in many places there may be
seen considerable quantities of petroleum where no gas escapes. •
At Laona, petroleum and gas both escape from the surface, and from the rocks and earth
beneath the stream; and there are several other localities where the same phenomena may
be seen along the outcrop of the sandstone, which is quarried on the line of the railroad.
Near Forrestville there is a copious discharge of this gas, which it is contemplated to convey
to the village for the purpose of lighting it. The village of Fredonia is lighted with this gas,
which issues from the shale forming the bed of the stream passing through the place. The
light-house at Portland harbor is illuminated with this gas, which rises from a stream three-
fourths of a mile north. - * -
In the conclusion of this chapter, I would say, that while I have intended to omit nothing that
can be regarded as important to theinterests of the inhabitants, or aiding them in the knowledge
or direction of their available wealth, I have omitted details which can be of no present utility,
and which may, by seeming to attach undue consideration to things which are only contingent
and prospective, have a tendency to mislead. For example, masses of beautiful stone, mar-
ble, beds of peat, marl, etc, I have not calculated by the cubic foot or yard, as if already
worked out and sold; whence the farmer or speculator, regarding only the ultimate value of
his wealth, increases his price according to this essentially false estimate. For it must be
considered that years are required to consume a marl bed, a peat bog or a marble quarry; that
the income depends on the demand; and though its stated value may be realized in twenty
or fifty years, the capital invested in its purchase might, in the mean time, and otherwise em-
ployed, yield fourfold. Like the products of a cultivated farm, the returns are constant and
slow, differing from that only in the circumstance that it is not inexhaustible. -
I would not be understood as attaching little importance to such property. To the farmer,
the value of a marl bed or a peat bog is immense; but I would say, that geologists, when
occupied in such objects as calculating the value of a mass, in dollars, while they degrade
their science, defeat their own purpose; they mislead those who are guided by their repre-
sentations, and foster the very spirit which their researches should allay, viz. the mania of
speculation. If such a course is pursued, it requires no great foresight to perceive that want
of confidence will prevail, and geology be ranked with the art of the adventurer with the mi-
neral rod. Besides, there is confessedly room for error in estimating the contents of a bed
or vein. In the fourth district, we know that beds of limestone, marble, grindstone grits, etc.
are liable to thin out within a few rods, or they may continue for miles: in this state of the
case, it is very unsafe to predict or infer that one stratum will extend for a distance of several
miles because another one has been found to do so, when we know the greater number do not.
The available resources for agriculture and trade, of the northern range of counties, consist
in iron ore, gypsum, marl, muck, limestone, sandstone, etc. Those of the middle range con-
sist of gypsum, limestone, marl, muck and some less important objects.
In the southern range, sandstone for all purposes of building, marl for lime, and muck for
improvement of the soil, are the principal resources. The inflammable gas is turned to some
CHAUTAUQUE COUNTY. 499
account in a few places, but no mineral wealth can be expected from any part of these coun-
ties. The products of the soil are the great source of prosperity in this district, and the
region is abundantly fertile to supply all the reasonable wants of man.
In order to follow out the plan, and to accomplish the objects of this work, it now remains
to trace the New-York rocks in their western continuation, to show some of the changes un-
dergone throughout their immense extent, the different phases under which they are to be
sought and recognized, and the influence of such lithological variations manifested in the
character of the imbedded fossils.
63*
500 GEOLOGY OF THE FOURTH DISTRICT.
CHAPTER XXIII.
On the identity of the Rock Formations of the Western States with those of New-
York.” ~
Knowing that the different rocks and groups, as developed in the Fourth District, extended
far to the westward, covering vast tracts of country, it was natural to feel a desire to examine
them more minutely, and to draw my own conclusions from personal observation regarding
their relative position. In the year 1841, I undertook a tour through the Western States, as
far as the Mississippi river, having for my object the identification of the rocks and groups of
New-York with those to which different names had been given by the Western Geologists.
No extended attempt of this kind had been made from actual examination and comparison, so
far as I know; and the inferences from published reports, and the occurrence of certain fossils,
had not proved satisfactory. The formations of the West, as described, did not correspond
with the order as established in New-York; and the discrepancy could only be accounted for
by supposing the thinning out of some important formations, or the occurrence of others not
there existing.
The similarity of some of the western formations with those of N ew-York, was first pointed
out by Mr. Wanuxem, whose observations were published in the American Journal of Science
and Arts in 1829. He identified the lower rocks of Ohio, Kentucky, and Tennessee, with the
Trenton limestone, from the occurrence of many of the same genera and species of fossils
common to both. I was referred by him to some localties which were important in settling
the questions of identity or difference, and I am indebted to the same source for information
of the existence of the Birdseye and Trenton limestones at Frankfort in Kentucky.
Having, in New-York, adopted certain subdivisions or groups of the strata, which are
strictly in the order of nature, it became a matter of much interest, to ascertain how far the
same subdivisions would hold good in distant localities, where there was evidently great
change in lithological characters. In employing geographical names for groups or individual
rocks, it is desirable to know the locality of greatest development for the whole country; and
when this is ascertained, the name should be adopted. But until the extent and comparative
development of each rock is known, perfect local names cannot be prefixed; and as a step
* This article is essentially extracted from a paper published in Transactions of the Association of American Geologists and
Naturalists, Vol. 1, page 267.
ROCK FORMATIONS OF THE WESTERN STATES. 501
toward the perfection of this nomenclature, the place of greatest development in the district
under consideration should give the name.
This examination westward also afforded a good opportunity of testing the value of fossil
characters, when applied to the same strata extending over wide tracts of country; and the
results will be seen, as we proceed, to have been mostly satisfactory. The value of litholo-
gical characters at the same time was found to fail in a great degree, and though in some
cases persistent, yet alone they would be found insufficient, and often lead to erroneous con-
clusions. From the investigations made in New-York, we had learned that groups, which
at one extremity of the State are of great importance and well characterized by fossils, cannot
be identified at the other extremity; and the same is more emphatically true of single rocks.
The Niagara group, so well defined by the topographical features of the country, as well
as by both its fossils and lithological characters, no one has yet attempted to identify to the
east of Little-Falls. Almost the same may be said of the Onondaga salt group and the Me-
dina sandstone; while on going in the opposite direction, we find several important members
of the Helderberg series entirely wanting west of Cayuga lake, and the Oriskany sandstone
existing only in patches here and there.
The undisturbed range of these deposits, with the great extent of unbroken outcrop bor-
dering the Ontario valley and its continuation along the Mohawk, has enabled us to acquire a
very perfect knowledge of the changes in the character of strata in their east and west exten-
sion. While such changes have taken place in important groups, others of less apparent
importance and of much less thickness are found remarkably persistent.
In making my examinations westward, the groups and individual rocks of New-York, as
adopted in the annual reports, were made the basis of reference.
The Lake Erie shore, from the New-York and Pennsylvania line (a point to which pre-
vious investigations had extended) to Cleveland, presents nothing of peculiar interest, being
occupied by the rocks of the Portage group, which for the most part are destitute of fossils,
except the remains of marine vegetables and a few Goniatites. The accompanying section
(Pl. XIII) extends from Cleveland to the Mississippi river, and no rock is represented which
was not actually seen. Westward, from Leavenworth, Indiana, it passes a little north of
the line examined, in order to present the great limestone formation on the Mississippi, as a
more prominent feature than further south, it being low and obscure near the mouth of the
Ohio.
The rocks seen near Cleveland, Ohio, are perfectly identical with those of the middle por-
tion of the Portage group, or Gardeau flagstones, being a continuation of the same as traced
from New-York along the lake shore. In following the road to Cuyahoga falls, the Portage
sandstone, or upper part of the group, is seen at Newburgh, and is there underlaid by green
shale. These are equivalent to the Waverly sandstone of the Ohio Reports, as was after-
wards ascertained by visiting the quarries at Waverly. From Newburgh we pass over the
shales and sandstones of the Chemung group, till we arrive upon the conglomerate which is
well developed at Stow and Cuyahoga falls.
502 GEOLOGY OF THE FOURTH DISTRICT.
This conglomerate, which, so far as I could discover, is identical with the outliers of a simi-
lar mass in the southern part of New-York, is the fundamental rock of the great Coal forma-
tion throughout the greater part of the western country, appearing everywhere, either as a
coarse sandstone or a pebbly mass, and affording an unerring guide to the proximity of coal.
Some portions of the mass at Cuyahoga falls are destitute of pebbles, and furnish a fine red-
dish or brownish sandstone, used for building. The greater part, however, is composed of
coarse materials, with white quartz pebbles. This character is exhibited in great perfection
along the road from Stow to Cuyahoga falls, and in the vicinity of the former village. Just
below the falls, its junction with the shales and sandstones of the next group is well exhibited.
In the lower part of the conglomerate, at this place, my friend, Mr. Newberry, has obtained
a large number of fossil plants, with the fruit of several species. They are imbedded in a
friable brown sandstone, highly stained by iron, and though mostly casts, are in a state of
good preservation. I afterwards obtained some similar fossils, from conglomerate near Deer
creek, below Leavenworth, Indiana.
Although usually destitute of fossils, this conglomerate possesses some characteristic marks
which may serve to distinguish it at very distant points. Among these, in New-York, are
thin seams, often apparently concentric, of hydrated peroxide of iron, crossing the mass at
various angles, or curved and contorted. Sometimes these appear as small nodules which
desquamate on exposure, or when struck with the hammer. In such cases the outer portions
only are composed of the hydrated peroxide, while the inner part is still a carbonate of iron,
the change having probably been effected by the percolation of water. At Cuyahoga falls, I
saw some beautiful exhibitions of these iron seams, and this character continues in every locality,
in greater or less degree, as far as examined westward; the ore frequently forming nodules
or accretions.” From what I was able to learn from other observers, in Michigan, there is a
considerable quantity of similar ore in the same situation in that State.
In the vicinity of Cuyahoga falls, the conglomerate may be seen passing beneath the coal
which is worked in several places in that neighborhood; the principal mines which I saw, are
those on the farm of Henry Newberry, Esq. Below the falls the Chemung group is distinct-
ly characterized, containing, however, few fossils compared with the same further east. I
obtained enough to convince me of its identity, and I have since received from Mr. Newberry
several others, which at that time I did not see. The most abundant fossil is a species of
Strophomena. Beside this, there is an Atrypa, a Cypricardia, an Orbicula, a Lingula, a
'small Crinoid, and one or two undescribed forms.
At Akron, the rocks of the Chemung group appear beneath the conglomerate, which is
there in its lower part a coarse grey sandstone. The same fossils as before noticed, occur on
a small stream by the side of the canal, below this village.
Passing south from Akron to Greentown, I came to beds of coal, succeeded by a dark-
colored shaly limestone, which abounds in fossils. Among these were two or three species
* See the description of this rock, chapter vii, pages 287 and 288, of this Report
Rock ForMATIONS OF THE WESTERN STATEs. 503
of Delthyris, several of Atrypa, a Productus, and crinoidal joints in great numbers. A lime-
stone holding this position among the coal beds is a very interesting circumstance, when taken
in consideration with the absence of any limestone representing the Carboniferous of Europe.
One species of the Delthyris, also, is very similar, if not identical with Sowerby's figure of
Spirifera attenuata; and the other fossils have all the aspect of those figured by Sowerby
and Phillips from the Carboniferous limestone of England. A similar rock appears in the
southern part of the State, where I obtained some of the same as fossils at Greentown. It also
appears in several places in the vicinity of Canton. -
Passing to the south and west along the road to Columbus, we soon leave the Coal forma-
tion, and come upon the groups below. These present few important features, except a
gradual thinning in that direction, and the almost entire absence of fossils. The Chemung
becomes scarcely distinguishable from the Portage group, and both are known in the Ohio
reports as the Waverly sandstone series. From beneath these, pass out all that remains of
the Hamilton group and Marcellus shales, the whole known as the black bituminous shales
of the Ohio reports, and possessing, as a whole, the character of the Marcellus shale of
New-York. I was not so fortunate as to meet with fossils in any part of this mass examined,
though they do occur in some places. This rock was traced nearly to Columbus; and a short
distance to the west of that place, the Corniferous limestone of New-York appears, presenting
its characteristic fossils. This mass is the upper part of the Cliff limestone formation of Dr
Locke, the name by which it is generally known in Ohio.” The localities where I saw this
rock exhibited less hornstone than is usual in New-York, but the position and fossil charac-
ters were unequivocal. - - -
After ascertaining the existence of the Corniferous limestone, and the middle and lower
members of the Cliff limestone, for some distance west of Columbus, an offset was made
into the coal region of the southern counties, and the line of observation again taken up on
the Ohio river at Portsmouth. - - -
In following down the river, the limestones appear rising from beneath the shales, as re-
presented in the section. Numerous localities are presented in the river bank and ravines,
where the blue limestone exists in great force; the most interesting, before reaching Cincin-
nati, are in Adams county, Ohio, and Maysville, Kentucky. An examination of the fossils
at Maysville convinced me of the identity of the Blue limestone of Ohio, and the Hudson-
river group of New-York. The evidences of this identity are the following: The mass con-
sists of green shale or marl, alternating with courses of bluish crystalline limestone of a peculiar
aspect, resembling that associated with the Clinton group of New-York, particularly the
portion containing Pentamerus oblongus. Thin layers of grey sandstone occur, sometimes
separate, and at others attached to the limestone in wedge-form masses, and always containing
a species of fucoid, which I had learned to consider a characteristic fossil in New-York.
* See Report on the Geology of the southwestern counties of Ohio, by Dr. JoHN LocKE. Ohio Geological Reports, 1838.
504 - GEOLOGY OF THE FOURTH DISTRICT.
Further examinations brought to light the Pterinea carinata, two or more species of Cypri-
cardia, a Strophomena, Cyrtolites ornatus, and the Bellerophon bilobatus, as well as the
abundant little shell (Orthis testudinaria 2) Orthis striatula. The latter fossil ranges through
the Hudson river group in New-York, as it does through the Caradoc sandstone of England.
This association of fossils, with the peculiar aspect of the limestone, and the presence of sand-
stone with fucoids, seemed indubitable proof of the position of this mass. Neither the cha-
racter of the rocks, nor of the fossils, indicates the Trenton limestone to which heretofore it
has been referred. Numerous other fossils, unknown in New-York, are found at Maysville,
the most abundant being several species of Orthis and Delthyris.
The cliffs of Cincinnati were next examined, and the same evidence, in a higher degree,
brought forth. At this place I met Dr. Locke, who gave me every information relative to the
limits of the two formations, Cliff and Blue limestones, as known in Ohio, and I afterwards
derived great assistance from his Report on the Geology of this part of the State. I was also
fortunate in meeting, at this place, with several gentlemen who were zealously engaged in ex-
ploring the rocks of the vicinity, and who voluntarily aided me in my objects. From Mr. J.
G. Anthony, Mr. Clark, Mr. Carley, and Mr. Buchanan, I received many characteristic fos-
sils of the locality. ' -
The section made there at this time presented the following features:
On the Kentucky side of the river, at the water level, (May 8th, 1841,) the rock seen was
a green shale with thin laminae of crinoidal limestone, containing few fossils. Among these
the Triarthrus Beckii is the most prominent, and with fragments of Isotelus, and a few imper-
fect shells, were all that I obtained. In New-York, the Triarthrus is never found below the
Utica slate, and is a characteristic fossil of that mass; though it does occur somewhat rarely
in the lower part of the Hudson river group. Taken in connection with other circumstances,
and the character of the fossils in the succeeding rocks, it seems a fair inference that this is
the equivalent of the Utica slate, or at least not far above it. -
At low water, on the Ohio, a lower rock appears; and though the specimens I have seen
contain no unequivocally characteristic fossils, of the Trenton limestone, yet it may exist here,
and Mr. Vanuxem informs me that he saw it in the valley of the Little Miami, a locality which
I did not visit.” - -
Proceeding upward from the green shale with Triarthrus, we find a somewhat similar shale,
with thin layers of sandstone, characterized by the presence of Trinucleus and Graptolites.
Still above this we find alternations of shale, or marl, and limestone, with Orthis striatula in
great abundance ; with this shell and above it occur Strophomena sericea, S. alternata ?
Pterinea carinata, Cypricardia angustifrons, C. modiolaris, Cyrtolites ornatus, with a great
* Very careful and extensive examination is often necessary, in order to identify rocks by the presence of characteristic fos-
sils. In the rocks of Cincinnati, Maysville, and other places, occur fossils of the Trenton limestone. Among them are Orthis
striatula, Strophomena (Leptaena) sericea, S. alternata ? Bellerophon bilobatus, Favosites lycoperdon, and others. The last named
fossil occurs with Bellerophon bilobatus and Orthis striatula in the Caradoc sandstone of England. The Calymene of these rocks
at the West, usually considered identical with the Trenton species, is probably distinct.
Rock ForMATIONS OF THE WESTERN STATES. 505.
abundance of corals and other fossils. Among these are Bellerophon bilobatus, Orthoceras,
and two or more species of Orthis similar to, or identical with, those of the Caradoc sandstone
of England. Fragments of Isotelus are abundant, also a species of Calymene.
From the enumeration of some of the forms, it will be perceived that we have here an as-
semblage of fossils similar to that of the Hudson river group of New-York. For here, as in
Ohio, the shales, with Triarthrus, are succeeded by green shales and slaty sandstones con-
taining Trinucleus and Graptolites, with other fossils. The Orthis striatula, O. callactis,
Strophomena nasuta, Pterinea and Cypricardia, are likewise characteristics of this group, as
well as Bellerophon bilobatus and the same species of Orthoceras. Strophomena sericea
occurs in Ohio, completely covering the surface of thin layers of limestone, as in New-York.
In both places are seen thin courses, composed almost wholly of the stems of Crinoidea, and
the species appear to be identical. - -s -
The remains of Isotelus, several species of which occur, have always been considered
sufficient proof of the identity of this rock with the Trenton limestone of New-York, and
these fossils have been chiefly relied upon. All the specimens which I saw, however, are of
different species from those of Trenton. So that although certain species of this genus do
occur in the Trenton limestone, and are characteristic of that formation, others are not neces-
sarily so; and unless we take wide ranges in our groupings, we cannot depend on generic
types. In this case the amount of evidence appears to be about equally divided between the
Trenton and Hudson river groups; but since there are fossils decidedly typical of the latter,
and since we know that in New-York they never occur in a lower position, we are compelled
to admit that this formation is of the same geological age.
Besides the fossils enumerated, are many which do not occur in New-York; among these
a beautiful crinoid and several species of Delthyris, Atrypa and Orthis. It should not be
omitted, that in the hill-side at Cincinnati, we find, attached to the limestone beds, numerous
thin wedge-form layers of sandstone, which usually contain a species of fucoid similar to one
in the Hudson river group, and the same as that noticed at Maysville. Besides the fucoid, this
sandstone contains a species of Strophomena similar to one of the same group in New-York.
From the evidence here adduced, it appears that in the West there is not so great a transi-
tion from the Black river and Trenton rocks to those above, as in New-York; and that, from
the fact of the greater similarity of lithological character, and the occurrence of many impor-
tant fossils, specifically and generically similar, throughout the mass, we may yet be inclined
to consider the whole as one great natural group, exhibiting well defined lines of minor sub-
divisions. The termination of the Hudson river group, in New-York, is the first point of
marked and unequivocal change in the fossil characters. Below this point there are many
forms which pass from one rock to another upward, often rendering it almost impossible to
decide what are to be considered as typical. In every case, however, certain species are en-
tirely limited to the mass they occupy. The great range of some of these species through
the lower rocks, with their total extinction at the termination, indicate a great change in the
condition of the ocean. Such a change is further corroborated by the occurrence of a thick
and extensive mass of conglomerate, which succeeds the Hudson river rocks in New-York,
[GEOL. 4th DIST.] 64
506 GEOLOGY OF THE FOURTH DISTRICT.
giving evidence of a period of disturbance. These suggestions are offered, not with any view
to merge in one formation what can be regarded as decidedly distinct, but with the desire to
offer some facts toward the foundation of general groups or classes, to which all the numerous
minor subdivisions may be referred. -
The junction of this group with the cliff limestone cannot be seen in the neighborhood of
Cincinnati; but in passing down the river, the two appear in juxtaposition before reaching
Madison, Indiana. In the Ohio reports, Dr. Locke refers to this place as exhibiting, in a very
perfect manner, the contact of the two rocks, cliff and blue limestones, which are well seen
in the deep cutting for the railroad one mile southwest of the village, and in a ravine still
further below. - -
The fossils of the blue limestone at this place illustrate the same view as at Maysville and
Cincinnati. The Pterinea carinata, with one or two species of Cypricardia, are common;
while Strophomena, Orthis, and others, abound in the middle portions, together with the
Atrypa capaw of Conrad, a species not seen at Cincinnati. Large numbers of Cyathophylli
occur of a species different from any of the higher rocks. Near the junction of the blue and
cliff, which latter is strongly contrasted in color, as well as other characters, there occurs a
stratum of twenty-five feet thickness, of a greenish grey sandy shale, containing Cypricardia
modiolaris, and numerous spherical masses of coral, (Porites ?) which lie in two courses, or
ranges, near the top of the mass, and separated by a few feet of shale from each other. Some
of these masses attain a large size, being three or four feet in diameter, while others are but
a few inches. -
The lower member of the cliff limestone, at this place, is a calcareo-siliceous mass, with
green stripes and spots, and crumbling on exposure to the air. It appears quite destitute of
fossils, so far as I could discover. About fifty or sixty feet above the base of this mass, I
noticed a strong ferruginous exudation; but the point being at the junction of the rock with
the loose materials above, I was unable to discover any ore in place. This rock, which
plainly succeeds the shales and limestones equivalent to the Hudson river group, is marked
by patches and laminae of green shaly matter, strongly resembling some portions of the inter-
mediate mass between the Medina sandstone and the Clinton group, being an intermixture of
the green shale of the one, and the sandy matter of the other.
Time, however, did not admit of going into detailed examinations, regarding the individual
rocks, or groups, composing the cliff limestone, the object being a general identification of
larger subdivisions. From examinations made at a short distance from this place, I learned
that the friable sandy mass just noticed was succeeded by a harsh, porous limestone, appa-
rently magnesian in composition, and possessing the general characters of the Niagara lime-
stone in New-York. At this place I was unable to find any fossils save a few crinoidal
columns, which gave to the rock much the appearance of the lower part of that at Niagara
falls and Lockport. The examinations of this rock in other places, where I found fossils,
and was able to trace the succession upwards, left no doubt of its identity with the Niagara
rock.
It should be remarked, that soon after leaving Cincinnati, the rocks are seen to dip to the
ROCK FORMATIONS OF THE WESTERN STATES. 507
west or southwest; and at Madison, the base of the cliff limestone has approached within
one hundred and fifty or two hundred feet of the river. From this point it continues to dip
in the same direction, gradually approaching to the river level, and finally disappearing be-
neath it at Louisville, or the Falls of the Ohio. The river, at the time, being high, did not
permit an examination of the rock directly at the falls; but the excavation of the canal below
Louisville has developed, in the loose fragments, the character of the rock, which consists,
apparently, of the water lime, and perhaps some portion of the Onondaga salt group, with
the limestones above. The most satisfactory exhibition, however, was a few miles further
up the river, where the rocks are very well exposed. Along the line of railroad, and in
the banks of a small stream, about three miles from Louisville, the same rocks are seen. The
highest mass at this place, contains a species of Calymene" characteristic of the corniferous
limestone of New-York, as well as several shells equally so; among these, a peculiar variety
of the so called Atrypa prisca, and a species of Strophomena; both shells are confined to
this mass. Below this was seen a rock with Favosites and Cyathophylli, which could be
identified with no other rock than the Onondaga limestone, possessing all its essential features,
both as regards lithological and palaeontological characters. Passing from this over strata re-
sembling the lighter colored portions of the water-lime series of New-York, we came upon a
drab-colored mass, in thin layers, abounding in Catenipora and Favosites; and below this a
lighter or ash-colored limestone, in thick Čourses, destitute of fossils. Such, simply, was
the order in which the rocks were examined at this place, and from which collections were
made. - -
From the examinations made here, at Madison and other points, the unavoidable conclu-
sion is, that in the cliff limestone we have the Helderberg series of New-York; or at least
the two persistent members, Onondaga and Corniferous, with the Water-lime, and, perhaps, a
meagre representation of the Salt group, together with the Niagara limestone. It seems con-
clusive, therefore, that the Cliff formation, as defined in Ohio, embraces all the existing for-
mations from the Corniferous limestone to the Clinton group inclusive, that formation having
been detected in this State, and one of its most important fossils in New-York (Pentamerus
oblongus) is abundant in Indiana and Iowa. -
After making these investigations in the vicinity of Louisville, I had the gratification of
seeing, in the cabinet of Dr. Clapp, at New-Albany, many of the fossils common to the rocks
of New-York, and which fully confirmed my views relative to the position of those examined.
These fossils were principally from the rock at the falls of the Ohio. From comparing my
observations of other rocks with those made by Dr. C., I became still further convinced of
the identity of different portions of the formations of the West with those of New-York,i and
that the limits of many of the rocks were as well marked there as at the East.
* Calymene crassimarginata of this Report, page 172.
* From a letter of Dr. CLAPP to the Philadelphia Academy of Natural Sciences, dated February, 1842, I am happy to see that
his views regarding the identity of the rocks of that region with certain formations of New-York, essentially correspond with
what I had expressed in the American Journal of Science of January preceding.
64*
508 GEOLOGY OF THE FOURTH DISTRICT.
Above the limestones last described, we meet with a “black bituminous shale,” which, from
position, seems to be the equivalent of the Marcellus shale of New-York," and is the only
representation of that rock, the Hamilton group and Genesee slate; for we pass directly from
this to the green shales and slaty sandstones of the Portage group or Waverly sandstone
series of Ohio. In the examinations made in these rocks for several hundred feet upwards,
no change from the Portage to Chemung groups could be identified, fossils for the most part
being absent. I should not omit to state, however, that in passing beyond these greenish
slaty rocks to a more micaceous and ferruginous yet friable sandstone, I found several shells
which bear close analogy, if not absolute identity, with the Chemung species. But finding
afterwards, in other parts of this sandstone, shells evidently belonging to carboniferous types,
I was led to question the inference as to absolute identity. Further investigations proved
that this sandstone, in passing upwards, became interstratified with beds of limestone, and
thin courses of oolitic limestone with fossils occurred in several places. These latter were
not persistent, but in some places several inches thick and soon disappeared entirely, or left
only a line of calcareous matter, marked by the presence of Producta. Still higher in this
rock are some quarries, where a mass of limestone eleven feet thick is wrought for building
stone. The lower part of this mass is a compact oolite, while the upper is rather coarsely
crystalline with fragments of fossils. Below this, and separated by a course of sandstone
of several feet in thickness, is another thick bed of limestone, and the whole is succeeded
above by sandstone like that below. The height of these quarries above the black shale is
four hundred and fifty-four feet; and the thickness of shales and sandstones between this
point and the main limestone above, is fifty or sixty feet more...f -
These rocks I had denominated subcarboniferous; and although the fossils and the character
of the intercalated beds of limestone indicate the commencement of the same era as the car-
boniferous limestone, yet it requires that a limit should be fixed between what is to be strictly
referred to the carboniferous period, and older deposits. The grey sandstone here spoken of
contained, in numerous localities, a large species of Productus, resembling P. hemispherica, a
carboniferous fossil; while there seemed to be a gradual transition from rocks of the Chemung
group to those above, indicating no cessation of deposition, and scarcely a change in litho-
logical character, except the occurrence of thin beds of limestone.'
* Near New-Albany, this shale is one hundred and four feet thick; “in other situations it is only fifty'feet thick.” — Second
Ann. Rep. of Geological Survey of Indiana, p. 15. - .
f The fossils referred to as similar to those of Chemung, are a species of Delthyris, a Strophomena, an Atrypa, and an Ino-
ceramus. After examining a more extensive collection from the same situation, made by Mr. W. C. Redfield in Medina county,
Ohio, I find that there are several species identical with those of the Chemung group in New-York, and others which are entirely
distinct. *. -
# The thickness given was ſurnished me from the surveys of road engineers in a letter from Dr. Clapp, of Sept. 2d, 1842.
§ I find, in reference to the Report of Dr. Owen on the Geology of Indiana, that he has denominated the rocks here described,
as well as the succeeding limestone, “Subcarboniferous.” The limestone following is denominated in its different parts by Dr.
Owen and Dr. TRoost, as Oolitic, Pentremital and Archimedes limestone.
ROCK FORMATIONS OF THE WESTERN STATES. 509
Pursuing my investigations down the Ohio from this place, I found that the grey sandstones
with intercalated limestone were succeeded by a thick and persistent mass of limestone, pre-
senting features unlike any of the limestones seen in New-York or Ohio. By reference to the
section, this limestone will be seen extending eastward to the vicinity of New-Albany, Indiana,
and passing beneath the level of the river, near Leavenworth, about fifty miles below. It is
visible, forming a cliff along the river, for nearly the whole of this distance, where it passes
under the conglomerate, or its representative, a coarse grey sandstone, showing diagonal lines
of deposition, with seams and nodules of hydrate of iron. This limestone reappears upon
the river in several places between Leavenworth and the Wabash, at some of which exami-
nations were made. Beyond the Wabash it reáppears and continues to the Mississippi river,
forming a low cliff often for many miles in succession. On the Mississippi, above the junc-
tion of the Ohio, it soon appears, forming at first but slight elevations, but soon rising into
cliffs of from one hundred to two hundred feet in height. It presents this character of cliffs
nearly to St. Louis, beyond which place it does not rise so high, but continues in view as far
as the Rock river, and extends up this stream beyond Dixon's ferry. From this rapid sketch
it will be seen, on reference to the map, that this limestone occupies an extensive area east of
the Mississippi river, and stretching westward its limits were unknown. On the south of the
Ohio it is known to extend into Tennessee, and from the Reports of Prof. Rogers, it is a very
extensive and important rock in Virginia. It thus becomes equally important with any of the
great limestone formations heretofore described in this country, in regard to position and
extent. When it shall become more generally known, it will be found a prominent horizon
for the proximity of the coal strata, as, in its absence, is the conglomerate further east.
The examination of this limestone at Leavenworth, gave the following characters: The lower
part of the rock is compact and fine-grained, breaking with a smooth conchoidal fracture.
This portion has been used for lithographic stones, and for small pieces serves the purpose
very well. Above this portion the character is somewhat irregular, with light-colored chert
or hornstone, which is often translucent. I was unable to find any fossils thus far upward, in
the mass at this place. Above the cherty layers the rock becomes coarser grained or semi-
crystalline, and contains numerous fossils of the genera Delthyris, Atrypa, and large numbers
of the Pentremites. The most remarkable fossil of this portion of the rock, and which occurs
just above the fossils named, is the Archimedes of Lesueur, a singular coral, appearing as
an expansion somewhat like the Retepora" twisted spirally round an axis; or rather, the edge
of the coral, by thickening and folding, forms the axis. This curious fossil always holds the
same position in the rock, the character of which differs from that above or below, being often
ferruginous or yellowish in color and fine-grained. This portion of the rock contains, besides
the Archimedes, one or two other corals, and one or more species of Crinoidea.
This is again succeeded by a beautiful light-colored oolitic mass, containing numerous
fragments of fossils, the principal of which are Producta, some perfect specimens being
obtained. A Trilobite, a portion of the head of which resembles an Asaphus, also occurs in
* I am informed by Mr. LYELL, that Mr. LoNSDALE regards this fossil as a species of his genus Tenestella,
510 GEOLOGY OF THE FOURTH DISTRICT.
this part of the rock. It is a very persistent mass, being seen at numerous and distant points,
Its character as an oolite is as perfect as specimens from Bath, in England; and its chalky
and fissile nature, considered alone, would almost induce one to regard it as a more recent
formation. Its position, however, cannot be mistaken; for, about one mile below Leavenworth,
it is seen passing beneath the grey sandstone before mentioned. At this point, without any
intermixture of the two deposits, we pass from a pure oolitic limestone to an equally well
characterized quartzose sandstone.
This limestone was again examined near the mouth of Oil Creek, Indiana, where it presents
the same essential characters as described, and the same order of the parts. Opposite the mouth
of Little Blue river, on the Kentucky side, the junction of the limestone and conglomerate
presents a singular siliceous aggregate, containing abundance of shells, and having somewhat
the character of buhrstone. From this place to the Wabash, there was little of interest to be
seen ; the rocks approaching the shore in many places, indicated along the whole distance the
existence of the great Coal formation of the Illinois or Wabash basin. From the section, it
will be perceived that the Wabash flows in the depression of a synclinal axis, and from thence
the strata gradually rise to the westward. - -
The limestone soon rises from beneath the river level, and continues in view nearly to the
Mississippi, being obscured only by superficial accumulations. After ascending, the Missis-
sippi for some distance, the rock again appears. The great valley, or “American bottom,” is
bounded on either side by abrupt cliffs of this limestone : the river meandering in its course
from side to side, sometimes runs at the base of the perpendicular rock; while the opposite
side presents a broad level bottom land, covered for the most part with luxuriant forests of
primeval growth. These cliffs form some of the most picturesque scenery, and, with the
small shot towers upon the overhanging margin above, suggest the idea of stupendous castle
walls of cyclopean architecture, crowned with the sentinel’s towers. -
Between the point of its first appearance on the Mississippi and its final disappearance near
the mouth of Rock river, I examined it at numerous points, and always found a very uniform
lithological character, which alone is sufficient to distinguish it from all other rocks, and ena-
ble one to identify it with its commencement in Indiana. The fossils, however, are constant
and unerring guides, which leave no room for doubt. The rock, on fresh fracture, has a
peculiar light grey color, much of it crystalline ; while other portions are compact and fine-
grained, presenting the appearances described at Leavenworth.
At St. Louis I obtained several fossils, principally corals and crinoidea; all of which, so far
as I know, differ from those found in any lower rock. Dr. B. B. Brown, of St. Louis, politely
presented me with specimens of Producta, from his cabinet, which were found in that vicinity,
and which corresponded with the British P. Martini. Having since had an opportunity of
examining a small collection of fossils from the carboniferous limestone of England, in the
Lowell Institute, I found many of the same species as those of this great formation, leaving
no doubt of the identity of the two. The difficulties, therefore, in the way of comparing our
rocks with those of Europe, seem in a fair way to be cleared up; and we learn, that among
all our limestone formations, in the eastern part of the United States, the true carboniferous
RoCK FORMATIONS OF THE WESTERN STATES. 511
limestone is wanting, its fossils appearing only in a few places in shale and sandstones asso-
ciated with the coal strata. -
For the greater part of the distance along which this limestone was seen, it is but slightly
inclined, often appearing horizontal. The only deviation of importance noticed, is near Her-
culaneum, on the Mississippi river. At this place there appears to have been an extensive
uplift in a northeast and southwest direction, elevating the strata at an angle of thirty degrees;
and from the existence of one or two small islands, seems, at some remote period, to have
obstructed the course of the river. From the shallow water at this place, the uplift appears
to have been of more recent origin than the excavation of the river channel, otherwise there
appears no reason why the depth here should not be as great as in other places.
Along the Mississippi river the common fossils are a large species of Delthyris, with a
smooth Orthis or Atrypa, in form like the A. concentrica of the lower rocks, but larger; these
appear at numerous localities which I had opportunities of examining. Several species of
Productus, with the larger valve very much arched, and the upper one concave and slightly
wrinkled, are constant, and good guides for this mass. My friend Dr. Owen has figured some
of the common forms in the American Journal of Science." Residing upon this formation,
his opportunities of investigation are ample, and we may expect that his zeal will lead to the
full development of its interesting organic contents.
After leaving the carboniferous limestone, near the mouth of Rock river, the coal and as-
sociated rocks appear, and beyond this point the lower limestones; the intermediate rocks
not being seen. There is evidently either an abrupt synclinal axis, or fault, which has brought
up the lower masses. From want of sufficient time to investigate this point, I was unable to
determine the precise cause, or amount of change. The contrast between the two limestones
thus brought into proximity, is very striking; the grey or ashen color is exchanged for a brown
or iron-stained rock, harsh to the touch, and composed of small crystalline grains. The mass
rises in broken or detached knobs or pinnacles, presenting a ragged and irregular outline, in
place of the uniform cliff formed by the higher limestone. In tracing this limestone up the
river as far as Galena, its lithological character is the same as that of the middle and upper
portions of the Niagara limestone, and all its associations are the same. The cliffs in many
places, particularly on the river above Dubuque, have all the appearance of those at the Falls
of Niagara, so far as regards lithological character, weathering, etc. Above the town of Du-
buque, this rock (cliff limestone) rests upon the blue limestone, which, according to Dr.
Owen's statement, is much thinner here than in Ohio; but not having traced it to its termina-
tion below, I am unable to speak from personal observation. Specimens which I saw from
the lower part of this rock about Praire du Chien, indicate the presence of the Trenton and
Black river limestones, by the large Orthocerata and other fossils. From a section made by
Dr. Owen, it appears that there are beds of sandstone, interstratified with, and underlying
the blue limestone.
* Vol. xliii, page 14.
512 GEOLOGY OF THE FOURTH DISTRICT.
It is in the Cliff formation, as before described, that the lead ores of Illinois, Wisconsin,
and Iowa are found, a part only of the rock yielding these ores. This portion appears to
correspond to the Niagara limestone; the upper part of the “cliff rock,” which represents
the Helderberg series, being destitute of metallic veins. Although the rock contains few fos-
sils, these indicate its position to be the same. The Catenipora, which in New-York occurs:
far more abundantly in the Niagara limestone than in any other rock, is found here in great
abundance, with Aulopora and a few other fossils. The next fossiliferous group below the
lead-bearing rock on the Misisssippi river, is that corresponding to the Hudson river group. If
the Clinton group exists, it has there become so incorporated with the rocks above, as to be
overlooked as a distinct formation. This point requires examination, and it is possible that
some representative of the group may be found there. Being a very variable assemblage in
New-York, it would not be surprising to find it under another aspect, or even incorporated
with the Niagara group, as far west as the Mississippi. Its last appearance in New-York,
on the Niagara river, is in the form of a mass of limestone twenty-five feet thick, with about
four feet of shale below ; the limestone at this point has lost the sandy and impure character
which it has further east, and assimilates more with the lower part of the Niagara limestone.
The only fossil met with in this mass on the Niagara river, was the Delthyris radiata, which
is found extending through the shale above, and in the lower part of the limestone.
In crossing the country from Galena to Chicago, few opportunities offered of examining
the strata except at detached points. The only rocks seen on the direct route are the two
limestone formations, the lower including Niagara and Helderberg, and the upper the Carbo-
miferous; and, from the great extent of level country, I was unable to see the intervening
rocks.
I had an opportunity of examining the rocks on the northern and northeastern shores of the
southern peninsula of Michigan, but my observations were too cursory to admit of any thing
like a connected view of them. The limestones of the Helderberg series, principally the
Corniferous and Onondaga masses, form the rocks of many of the bays and harbors; charac-
teristic fossils of these masses being recognizable in those examined. At Mackinac, the upper
part of the Onondaga salt group, and possibly a small portion of the Water-lime group, form
all the rocks seen. The former is partially altered from its usual characters in New-York,
some parts exhibiting the large angular cavities, the whole appearance being that of a vesicular
mass; and had the cavities been spherical instead of angular, it would have been referred to
igneous origin. This mass being isolated, renders it difficult to trace its connection with those
appearing to the south and east of it; but from its great similarity to the Salt group of New-
York, and from its apparently passing beneath those representing the Helderberg series, no
doubt remains as to the propriety of this reference. -
The exhibition of strata along the line of the section given, illustrates some very interesting
points in the geology of our country, and proves the existence and order of succession in
certain rocks, and their equivalents over wide areas; offering us facts which will still further
enable us to solve the problem of the condition and character of the ocean during the earlier
geological periods.
Rock ForMATION OF THE WESTERN STATES. 513
The great extent of almost undisturbed strata affords an opportunity for the most satisfac-
tory investigations, throughout all this country. The anticlinal axis which is crossed by the
section near Cincinnati, is an important feature. By the elevation of this axis, the higher
rocks have been removed, and the two great coal basins of Ohio and the Wabash valley
(formerly in all probability constituting one) are thus separated from each other. This axis
extends in a direction northeast and southwest; and passing along the western part of Ohio,
and crossing Lake Erie near its western extremity, it gives origin to the numerous islands of
this part of the lake. It extends onward into Canada, and I understand from the Messrs.
Rogers, that they have traced it far northward in that province. To the southward it passes
through Kentucky and Tennessee, and at Frankfort, in the former State, elevates the Trenton
and Birdseye limestones above the level of the river. - ~ * -
The section crosses a synclinal axis which runs nearly parallel to the great anticlinal one,
but its extent is unknown to me. The Wabash flows in this depression, which brings the
coal-bearing strata below the level of the Ohio river, at its junction with the former. From
this point the strata are seen to rise to the westward as far as the Mississippi; but beyond,
little is known of them. From the occurrence of extensive coal deposits in Missouri, it may
be presumed that the strata decline to the southwest, but I have no data from actual observa-
tion on which to found an opinion. - - - .
From the necessarily hasty examinations made during this tour of exploration, which was
extended over a large area, it was impossible to give that minuteness of detail, which is desi-
rable before the subject can be considered complete. All that was attempted was to trace the
great groups of New-York westward, and, if possible, to identify them with those known by
different names in that part of the country. If any light has been thrown upon this question,
or if only some few points of identity have been established, the object will have been
accomplished. In this vast field there is room for all the laborers that can be found for half
a century to come ; and I doubt not, from the numerous and efficient observers now at work
in this region, upon their native or adopted soil, that all the most important details will soon
be wrought out. . -
From the want of a well defined and acknowledged basis in the West, it would always have
been difficult, if not impossible, to establish the identity from that direction eastward; and it
requires a knowledge of the New-York rocks, in their wide geographical range and undis-
turbed position, to settle satisfactorily the place of the western rocks. - -
From the facts here stated, the conclusion seems unavoidable, that the character of fossils
is, sometimes, as variable as lithological characters; in fact, that the species depend in some
degree upon the nature of the material among which they lived. Fossil characters, therefore,
become of parallel importance to the lithological; and, in order to arrive at just conclusions,
both must be studied in connection, and localities of proximity examined. In the cases of
the Hudson river group of shales and sandstones, in passing from New-York to Ohio, the
lithological character is almost entirely changed; and at the same time, also, the most promi-
ment and abundant fossils are unlike those of that group in New-York. More careful exami-
[GEoL. 4TH DIST.] - 65
514 GEOLOGY OF THE FOURTH DISTRICT.
nation, however, reveals the fossils which characterize this group at the east, and also at the
same time some obscurely similar lithological characters. Similar lithological changes,
accompanied by like changes in fossils, occur in more limited districts within the State of
New-York. - - -
The most marked and important changes, however, appear to be in the higher rocks of the
New-York system. The Hamilton group and Marcellus shale, which in New-York have a
thickness of one thousand feet, have diminished to one hundred where last examined; and
from being the group most prolific in fossils, as it is in New-York, it has become entirely
barren of them. The rocks forming the Portage and Chemung groups, which in their greatest
development in New-York are scarcely less than three thousand feet in thickness, and in
Pennsylvania much more, have, in Indiana, diminished to as many hundred. The upper of
these groups, from being extremely fossiliferous, has become almost destitute of these charac-
ters; so that, at the furthest extreme examined, they furnish but an equivocal guide. In these
groups, lithological character is more persistent than fossils, and it requires a knowledge of
the superposition to identify them satisfactorily. The greater thickness of these sedimentary
deposits, and the greater development of fossils occurring at the same point, proves the organic
forms to have flourished in a litoral position; and beyond these points, where the thinning of
the strata indicates a greater distance from the shore, the fossils diminish, and at the more
distant and deeper points are not found at all. There is no evidence of denudation in these
instances; and if there had been, the parts left would have retained the same fossils — had it
ever contained them—as they do further east. -
Throughout that part of the ancient ocean now occupied by Ohio, Indiana, Michigan, Illi-
nois, and even to the west of the Mississippi, there appears to have been comparatively a
small number of living forms existing from the period of the final deposition of the Helder-
berg limestones, to the commencement of the Carboniferous period; while in New-York,
during the same period, there were a greater number of forms and individuals than in all the
preceding periods. Without desiring to diminish the value of fossil characters as means of
identifying strata, it must still be acknowledged, that similar conditions in the bed of the ocean,
and, appararently, similar depth of water, are required to give existence or continuation to a
uniform fauna; and when we pass beyond the points where these conditions existed in the
ancient ocean, we lose, in the same degree, the evidences of identity founded upon fossils.
Some species, it is true, have lived onward through successive depositions, often of very
different nature; yet, at the same time, these may not have had a very wide geographical
range. In the case before us, some species have lived during the deposition of all the rocks
from the Hamilton through the Chemung groups, and yet they have never extended them-
selves as far westward as Ohio and Indiana, although the nature of the deposits there was as
favorable to their existence as in New-York. .
For the distance of one hundred or two hundred miles from the shores of the present con-
tinents, the forms may be similar—we know not but they are ; still, who can say what
changes may occur, or whether any exist in the depths a thousand miles from land? From
ROCK FORMATIONS OF THE WESTERN STATES. 515
the nature of sedimentary deposits, it can be only the finer parts that ever reach to great dis-
tances from their origin; and, reasoning thus, the fauna of the deep and distant parts of the
ocean, if any exist, would be uniform, not being liable to destruction or change of condition
from the rapid invasion of variable deposits like those near the shore. The deposition of a
coarse sandstone or conglomerate succeeding to a shaly mass, would in all probability destroy
the greater number of living forms as far as it extended. But at the same time, the finer
materials produced by the same cause, would extend far beyond the limits of the coarser; and
thus approximating, in some degree, to the lower mass, the fossils might be continued long
after they were destroyed at another point.
One of the most interesting changes in the products on going westward, is the great increase
of carbonate of lime, and the diminution of shaly and Sandy matter, indicating a deeper ocean
or greater distance from land. The source of the calcareous deposits is thus shown to have
been in that direction, or in the southwest; while the sands and clays had their origin in the
east, southeast and northeast, producing, during long intervals, a turbid condition in the waters
of these parts, unfavorable to the production of calcareous matter, and the formation of chemi-
cal deposits. In New-York we are evidently upon the margin of this primeval ocean, as indi-
cated in the character of the deposits as well as organic remains; the southwest unfolds to us
a portion of greater depth and more quiet condition.
65*
516 GEoLogy of THE FOURTH DISTRICT.
CHAPTER XXIV.
On the identity of the New-York Formations with those of Europe. Table of
equivalents in American strata.
Something has already been said upon the identity of the rocks of New-York with those of
Europe, and particularly with those of England and Wales. From the very fully illustrated
work of Mr. Murchison, we are made acquainted with many fossils holding the same relative
position in the rocks of England that similar species do in this country. The general litholo-
gical characters of many of the successive strata correspond with those of New-York, and it
is very natural that we should endeavor to find sufficient resemblance to identify them as of
the same geological periods. For the great systems this has already been done, and there
remains no doubt but the sedimentary rocks of New-York correspond with those of the Silu-
rean and Old Red systems, as described in the Silurian Researches. If the Devonian
is to be regarded as a distinct system, we shall find its representative in the Chemung and
Portage groups, with, perhaps, a part of the Hamilton Group. In New-York, however, as
already stated, no subdivisions can be made which are entitled to the name of systems.
In regard to the identity of minor subdivisions, some obscurity still exists; though there
can be no doubt of their correspondence, in all important particulars. When we more fully
investigate the organic contents of our rocks, we shall doubtless find many more species com-
mon to the strata on both sides of the Atlantic.
In the rocks of the United States, there appears to be a much greater number of fossils
than in rocks of the same age in Europe. In many instances, too, it happens that the typical
species, upon the other side of the Atlantic, are very rare or obscure in New-York and else-
where, and from the multitude of other forms, they might almost be overlooked. We have,
however, made great advances in identifying individual formations and strata, and our pro-
gress in this respect is very gratifying. - -
The following tabular arrangement corresponds, very nearly, with the relative position of
the rocks of the two systems in Great Britain and New-York:
NEW-YORK FORMATIONS COMPARED WITH THOSE OF EUROPE, 517
SubDivisions of THE Rocks of THE NEw-York SystEM. SUBDIVISIONs of THE SILURIAN AND OLD RED SystEMS IN
GREAT BRITAIN.
Old Red Sandstone. Old Red Sandstone.
Chemung group.
. Portage group. - -
Genesee slate. Upper and Lower Ludlow rocks, including the
Tully limestone. | Devonian System of Phillips.
Hamilton group.
. Marcellus shale. \ 2
. Corniferous limestone. Y
Onondaga limestone,
Schoharie grit.
. Cauda-galli grit.
. Oriskany sandstone,
. Upper Pentamerus limestone.
. Encrinal limestone,
. Delthyris shaly limestone,
. Pentamerus limestone. t
. Water-lime group.
. Onondaga Salt group.
. Niagara group. -
. Clinton group.
. Medina sandstone.
. Oneida conglomerate. } Caradoc Sandstone.
. Grey sandstone. !
. Hudson-river group. J
. Utica slate. Llandeilo flags.
. Trenton limestone. ~
. Birdseye and Black-river limestones. These formations are not as fully recognized in
e Chazy limestone. * Great Britain as in New-York.
. Calciferous Sandrock. 'i.
. Potsdam Sandstone,
1
1
1
> Wenlock rocks.
i
:
:
:
:
2
7
2
8
2
9
f
There are many reasons for including the Nos. 7, 8, 9 and 10 in those equivalent to the
Ludlow formation; but in some places, the upper of these contains fossils which are charc-
teristic of the Wenlock rocks.
The Niagara group is evidently referable to the Dudley period, which is a part of the
Wenlock formation. r
We are compelled to include in the rocks equivalent to the Caradoc sandstone, the Clinton
group, from the occurrence of Pentamerus oblongus in great numbers, and in a condition pre-
cisely similar to the same fossil in the impure limestones of the Caradoc formation. From
the occurrence of large numbers of fossils in the Hudson-river group identical with those of
the Caradoc sandstone, there remains no doubt of its equivalency with that formation.
518 t GEOLOGY OF THE FOURTH DISTRICT.
The Utica slate (and perhaps the upper part of the Trenton limestone) may be regarded
as an equivalent of the Llandeilo flags, mostly from similarity of lithological character; but
one or two fossils being known in New-York, which are identical with those of the latter for-
mation. - -
The formations below the Trenton limestone appear not to be recognized in England and
Wales, with the same distinctness, or in the same degree of development as in New-York.
They are probably equivalent to some of the rocks included in the Cambrian system, and
which doubtless will yet be more fully recognized.
That there should be important differences in the character of sedimentary deposits, at
such great distances, is not surprising; indeed, it is more astonishing that there should be
so great a degree of similarity, when we consider the circumstances under which they were
produced. It has been shown, in the last chapter, that upon our own continent, within the
distance of a few hundred miles, great changes occur in the nature of the sedimentary strata;
changes which almost prevent a recognition of the same formations, and which are at the
same time accompanied by a different association of organic remains, showing that the nature
of the sediment influenced the character of the living forms. Absolute similarity, therefore,
in all the lithological and fossil characters is hardly to be expected in any two points at re-
mote distances from each other. - -
The differences which the same strata present at distant points, and the comparative degree
of development which formations exhibit, have given rise to a diversity of nomenclature, in
different parts of the United States. The surveys in progress required the adoption of pro-
visional names at least, and these have been given, generally according to the nature of the
rock, or from some locality where its characters were best developed. From the different
Reports I have constructed the following Table, which may, perhaps, be of use in comparing
the formations of different parts of the country, and in reading the respective reports.
EQUIVALENTS OF AMERICAN STRATA.
519
Tabular arrangment of lower American strata, showing the equivalency of those known by
different names in the several States.
º
--> -- a--a * ºr
NEW-YORK SURVEY.
PENNSYLVANIA AND
VIRGINIA SURVEYS.
OHIO SURVEY.
*Suj.º-s “…º. º.º.º.º.º.º.º.º." - . 1. ‘ ºn 2 --> r2: ... … .º.º. -, *.*, *.x ºr : *, * * * * . . . . . .
#| 1. Potsdam sandstone. No. 1.
il 2, Calciferous sandrock. No. 2. Wanting.
*3. Black-river and Birdseye lime- 2 |
4 tº mºre. §3. |Blue lºstone and man
5. Utica slate. No. 3. ſ formation.
6. Hudson-river group. No. 3.
7. Oneida conglomerate. No. 4. Wanting.
8. Grey sandstone. No. 4. Wanting.
9. Medina sandstone. No. 5. Wanting.
10. Clinton group. No. 5.
11. Niagara group. Part of No. 6. Part of Cliff limestone,
(This formation is but P.
: tially developed in the Mackinaclimestone: gre
: 12. Onondaga salt group. * gº #: 3. } . and porous #.
i | sively in the northern SLOIſle,
: 3. W. l U part.
j| 13. Water limestone. - º o
§l 14. Pentamerus limestone. | Included in No. 6 ſº º
| 15. Delthyris shaly limestone. intº In No. 0, Wanti he Little lºverse bay
§ 16. Encrinal limestone. | if existing. | ..", *.*. . º: #.
§ 17. Upper Pentamerus limestone. J > States ester #. . U19
#| 18. Oriskany sandstone. No. 7. | - | * one in º .
| 19. Cauda-galli grit. No. 7. i. #. º Q Ul]] (162F
| 20. Schoharie grit. J U f the Cliff [ pay timestone
# 21. Onondaga limestone. er part of the Cli º º
il 22, Corniferous limestone. : º { Corniferous limestone.
§ 23. Marcellus shale. No. 8. ack Slate. ->
il 24, Hamilton grou No. 8 } Wanting, or but partially {* Black aluminous
: º group. • *-* g. developed. tº
# 25. Tully limestone. Wanting. B
| 26. Genesee slate. No. 87 Wanting ºf º
i (Soft, light colored sand- ||
: stones. Argillaceous ||
| 27. Portage group. } No. 9 } Waverly sandstone slates and flagstones of |
# 28. Chemung group. • * > * . Sel'10S. Lake Huron. Sand- ||
| Stones of Point Aux ||
U Barques. #
Wanting.
The State of New-York presents a better opportunity for defining the limits of the several
subdivisions of the system, than any point yet observed to the west and south. The different
members are more numerous, but at the same time they are usually well marked, either
by lithological characters or organic contents, and often by both together.
ble to adopt any subdivision of strata which shall hold good, and at the same time be easily
recognizable over wide areas; and under these circumstances, the more minute are our dis-
* I am not aware that these two rocks appear in Ohio, although they do in Kentucky, and the name adopted in the Ohio Re-
ports are intended to embrace them.
# I have been disposed to consider the Black slate or shale of Ohio, in some places, as a partial development of the Genesee
slate of New-York.
It seems impossi-
520 GEOLOGY OF THE FOURTH DISTRICT.
tinctions, the better able are we to seize upon obscure relations at distant points, and turn them
to our advantage in the identification of strata. We have learned that a formation which on
the Mississippi is a limestone, is, on the Hudson, a shale and sandstone; yet in the former
place we may detect some obscure traces of slate and sandstone, while in the latter we often
meet with beds of impure limestone. The same or similar changes occur in other formations.
In the names adopted thus far, there is nothing to prevent the formation of a harmonious
nomenclature for all our rocks; while to the inhabitant of New-York, and other States, the
local names with which he has become familiar may be retained and used without detriment
to the progress of the science.
CONCLUSION. 521
CHAPTER XXV.
CONCLUSION.
In concluding this Report, we are naturally led to take a retrospective view of the condi-
tion of the surface of this portion of our planet during the accumulation of these sedimentary
deposits. We behold a wide expanse of ocean, which received these materials from adjoining
land, and upon the bed of which flourished the myriads of living forms which were succes-
sively imbedded in the strata, until finally the whole emerged a vast continent from beneath
the sea. We find at one time the evidences of a quiet ocean, with clear waters, abounding in
corals and shells ; and at another, a turbid condition in which all these forms ceased to exist.
Long periods of repose were succeeded by disturbances which changed the whole scene, and
then followed new creations and new materials of deposition.
It is universally acknowledged among geologists, that these immense sedimentary deposits
could only have accumulated beneath the waters of the ocean, during an incalculable period
of time, long anterior to the present condition of the surface. Now in order to furnish mate-
rials for such formations, we must conceive of the existence of continents where no vestige of
them now remains; from the abrasion and destruction of these, and from the transporting
power of rivers and ocean currents, the materials composing them were reduced to the state
of pebbles, sand, and finely comminuted mud, which were widely diffused and gradually or
rapidly precipitated upon the ocean bed. The varying nature of the deposits proves to us
that these elevated lands frequently changed their condition or outline, or that new sources
of materials were opened to the destroying and transporting agencies. Sometimes, however,
there is little variation for a long time : the same sources supplied the material; the same
agents, with unchanging intensity, removed and distributed it widely over the bed of the ocean;
while, again, within a short period, its nature is entirely altered, or a new source brings in
matter of a different kind to mingle with the hitherto uniform deposit. The disturbing forces
that sometimes long slumbered, seem often to have broken out suddenly with renewed energy,
changing the whole condition in a short space of time.
[GEol. 4th DIST.] - 66
522 GEOLOGY OF THE FOURTH DISTRICT.
Notwithstanding all this, however, the unity of the series is never broken; and although,
during certain periods, all living things inhabiting the ocean were exterminated, the violence
and disorder that prevailed at the sources of these deposits never prevented the gradual and
quiet deposition at distant points. The change from one rock to another is rarely abrupt:
there is usually a mingling of the products of both ; and lime, sand and clay are found in all
their varying proportions. Still the great uniformity in mineral character of certain deposits
is very remarkable. The black and green shales of some of the higher rocks of the New-
York System can be traced over an extent of a thousand miles, while specimens from either
extremity are scarcely distinguishable. - -
The conditions of this ancient ocean bed are as clearly proved by the nature of these
deposits, as is the character of any small stream from the nature of the detritus it transports.
The varying depth is marked upon the strata, and the clear or turbid state of its waters is
indicated by the character of the formation and the kind of living things that then flourished.
We are able to recognize portions which were raised above the surrounding ocean, and even
the direction of the waves is as perfectly preserved as upon a modern sea beach.
The evidences of this condition have been pointed out as we progressed. We have seen
that the strata from the Hudson to the Mississippi are composed of materials which could
only have been deposited from water, and that they contain organic remains which could only
have lived upon the bed of an ocean. It is necessary, then, to conceive of a period when
all that portion of our continent, now occupied by these rock formations, was covered with
Water. -
The chief source of our sedimentary deposits must have been from the east or southeast;
and from this direction the sand of the earliest formation was distributed over the bed of
the ocean, together with fragments and pebbles of rock. Calcareous springs issued from
the margins of the sea, and mingled their products with the arenaceous matter. For a period
the abrading and transporting process was in a measure suspended, and corals and shells took
possession of the limpid waters of the ocean; these constructed their habitations, and lived
quietly through myriads of ages. Their perfect structures and comminuted remains constitute
a limestone formation which flanks the great primary nucleus of New-York, and, extending
into Canada, spreads out westward over almost the entire width of the continent. This con-
dition ceased with the deposition of the Trenton limestone; the bed of the ocean subsided, and
a deposit of carbonaceous mud rendered the waters turbid with its wide diffusion, while few
living forms existed during the period of its accumulation. Again the transporting power
became more energetic, or new sources were opened, and sand became mingled with the mud;
the latter gradually ceased, and gave place to sand alone ; and towards the close of this period,
the disturbing influences and the transporting power had reached their acme, and the forma-
tion is terminated by a coarse conglomerate, indicating a period of storms and tempests.
During this time were deposited the shales and sandstones of the Hudson-river group,
terminating with the Grey sandstone and Oneida conglomerate.
CONCLUSION. 523
After this a new source of materials is opened; and apparently from a mud volcano, in the
midst of this ocean, is poured forth rapidly a vast deposit of mud and fine sand charged with
ferruginous matter. No vestiges of living forms are found till towards the close of the period,
when the mud had in a great measure given place to sand; and here only a few appear. In
this period are included the marls and shaly sandstones of the Medina formation. To these
succeed finely levigated mud; but it soon alternates with arenaceous and calcareous deposits,
and even with coarse conglomerate over limited areas, showing the changing condition of
the ocean, and the nature of the sedimentary and chemical products. Large quantities of
hydrate of iron are spread over extensive areas, mingled with the fragments of organic remains.
The whole presents a group of Protean character, indicating the fluctuating nature of the
deposits, and the disturbance at the source of the materials. Still, over a large portion of
the country where it is exposed, the influence of those disturbing causes did not extend, and
we have all the phenomena indicative of a quiet deposit in a moderately deep ocean. Such
are the materials of the Clinton group.
The Niagara group commences in New-York with a deposit of finely comminuted mud,
while at the west it is almost entirely calcareous. Its attenuated northern and eastern extremity
in New-York reaches nearly to the Hudson river; while, pursuing it westwardly, it expands
to an enormous thickness, and covers a vast area in the valley of the Mississippi. For an
almost incalculable period of time, this part of the ocean bed could have suffered little change,
nor have been disturbed by inundations of sedimentary matter. The whole expanse must have
been one broad blue ocean, with its infinity of coral groves, among which lived the shells and
crustaceans; and here, in sheltered nooks, the crinoideans reared their beautiful and gorgeous
heads, and above them shone the bright tropical sun. But this period of repose is suddenly
broken ; the ocean bed sinks down, and an overwhelming inundation of mud is spread out over
a large portion of its before limpid waters. The whole family of corals, shells, and crustaceans
are alike exterminated. Nor is it mud alone that here operates as a destroying agent of the
organic forms; the deposit, doubtless ejected from a huge mud volcano, is charged with saline
matter, and corroding acids, which would alone destroy all organisms. This vast mass of cal-
careous mud formed the marls and shales of the Onondaga salt formation.
Towards its close, calcareous matter becomes intermingled in an increasing proportion, and
a few shells appear. At last the turbid ocean becomes clear, when again the corals commence
their habitations, and with myriads of shells, and crustaceans, continue through an immense
period of time, disturbed, it is true, by an inundation of sand and mud, forming the shale of
the Cauda-galli grit and Oriskany sandstone, which, in some parts within their range, destroyed
many of the living beings. This, of all periods, seems to have been the most prolific in its
growth of corals; and numerous species abound, not only throughout New-York, but far
westward to the Mississippi river, showing, over an extent of a thousand miles, a uniform
depth and condition of the ocean; and like the barrier reefs of modern seas, giving birth and
shelter to myriads of living creatures, whose destruction formed the rocky strata.
66*
524 GEOLOGY OF THE FOURTH DISTRICT.
With this condition of things terminated the Helderberg series of limestone, the last of the
important calcareous formations in New-York. The ocean bed again subsided, and a deposit
of dark mud was gradually precipitated upon it, while few organisms existed. Gradually
vitality increased ; the dark carbonaceous mud became intermingled with calcareous matter;
living forms were multiplied, and, if possible, became still more numerous than in any
preceding era; the sea emphatically teemed with life, and the individuals of many species
can only be enumerated by myriads. Soon, however, sand became intermingled with the fine
materials; a gradual change in the organisms supervened, and finally the sand predominated ; .
and throughout a long period, the accumulation consists of alternate deposits of argillaceous
and arenaceous matter, or an intermixture of both, the whole abounding in organic forms.
During this period were accumulated all the materials forming the Marcellus shale, the
Hamilton group, and the Portage and Chemung groups. At the termination of the latter, a
greater change supervened; and though the formations are not widely different, all the pre-
viously existing organisms disappear.
Look, however, at this time, to that great portion of this ancient ocean, now occupied by
the States of Ohio, Michigan, Indiana, Kentucky and Illinois, and even far west beyond the
Mississippi. From the period of the final deposition of the Helderberg limestone, to the com-
mencement of the Carboniferous era, this vast expanse was comparatively a solitude. Instead
of the busy multitude thronging every part of the sea farther east, this was cold, dark and
deep; presenting no beautiful corals, or the still more beautiful crinoideans, and with but few
of the shells of the eastern waters, it more resembled a primeval ocean where vitality had but
just assumed its place among the laws of nature.
Beyond the termination of the New-York system, we might follow the successive formations
through the Old Red Sandstone and Carboniferous periods, which exhibit the same changes
throughout, as before described. In the latter system, we perceive the formation of an im-
mense deposit of limestone at the west; while at the east, the ocean was accumulating only
sand and clay. The same general law will be observed to exist in all the previous formations;
the proportion of calcareous matter constantly augmenting, and the arenaceous and argillaceous
matter decreasing in a westerly direction.
Such has been the mode of formation of the successive deposits, forming the subject of this
Report; the operation of the same laws, and the influence of the same agents, as are now
active, have produced this stupendous accumulation of materials. Subsequent operations have
dislocated, elevated and overturned the indurated strata thus formed, and, together with the
action of water, have produced the modern detritus, the soil of the surface, the fragments and
transported boulders. - -
The description of each rock has shown that the increment of fresh matter has almost
uniformly been from an easterly direction, more especially of the purely mechanical deposits:
this, according to a well known law of physics, must have first produced expansion in that
direction, and consequently the eastern portion of our continent would first be elevated.
CONCLUSION. 525
This is proved by the subsequent formations; for while on the west the older rocks are exten-
sively overlaid by deposits of the age of the Cretaceous formation, we find on the east that
the Greensand of the same age occupies but a limited area, and but little elevated above the
tide water, leaving the extensive Palaeozoic formations overlaid by no newer rocks, except
in a few places and at low elevations by a recent Tertiary.
The same causes which have operated in the production of these formations are now active
in abrading the materials of our present continent, and transporting them into distant parts of
the ocean; and though we witness no such extensive or gigantic agencies of transport, as
must have existed during former periods, still the law is the same, and the ultimate effect
will be attended with like circumstances.
The changes here enumerated, are but a few among the great series of changes which
have brought the surface of the earth into its present condition; which have formed the moun-
tain chains, excavated the deep valleys, or piled up among its successive strata, materials
fitted for our use and instruction. Every successive change has left its monuments, upon
which is recorded the history of the past: that history shows the operation of a uniform law,
the influence of a mighty design in the construction of the stupendous fabric on which we
exist. And though we are not disposed to say, that the Creator has through all ages been
fashioning and preparing the earth for the abode of man, or storing up its mineral treasures for
his use alone, we can yet see the operation of his Divine law, and recognize in its harmonious
adaptation the result of ETERNAL BENEFICENCE AND ETERNAL WISDOM. -
TABLES
0 R G A NIC R EMA INS,
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE MEDINA SANDSTONE.
f
ILLUSTRATION No. 1. – No. 5, page 46 of this Report.
Figs. 1 and 2. Fucoides Harlani. This is the most characteristic and widely diffused fossil
of this rock. Its vertical range is very limited, holding a place usually near the
upper part of the mass.
No. 2. — No. 6, page 48 of Report. #
Fig. 1 and 2, Euomphalus pervetustus, HALL. Cyclostoma pervetusta, CoNRAD (Geologi-
cal Report for 1839, page 65); inadvertently written Pleurotomaria pervetusta at
page 48.
Fig. 3. Cypricardia alata, H. Unio primigenius, C. (Geological Report of 1839, page 66.)
Fig. 4. Orbicula parmulata, H. Lockport.
Fig. 5. Lingula cuneata, C. (Geological Report of 1839, p. 64.) Medina.
Figs. 6 and 7. Two views of Bellerophon trilobatus, Planorbis trilobatus, C. (Geological
Report for 1839, page 65.) Medina.
Figs, 8 and 9. Cypricardia orthonota, H. Unio orthonota, C. (Geological Report for 1839,
page 66.) Medina.
No. 3 – No. 10, page 52.
Lingula cuneata, as the shells appear when attached to the surface of sandy layers, in the
grey sandstone of Niagara county.
ORGANIC REMAINS OF THE MEDINA SANDstonſ.
No. 1.
§
X
=№
@%<g
§§-}// ±
§§§ģſº;
ſº
º
|;
ź
·ſº?
ºz.≤
§§
ſae
·ÑYW
ŅŠNNS（-J）
§§\\\$$§§§N
%
.. tº
º/
º
%
*}
º
%
É%
§§
ſaeſ）
% ），
}
%
%
§
j
%
¿?
ſ.№, ſãº: ¿?
sºffº， …：…， ¿ºs:
**，№.：، ،≡
ĶäsŞÈ№šģēŠN
ș.~
§¶√∞∞∞-
à
?
§
º
2%
§ās§È§§
- ~~§§
§§
%
%;
%
'$$
8
|ft
|
º
|
º:
š=2#.
|
§ |
§
- g
Šºš
Sº-º:
º-º-º-º:
º Ess==
ſae （ ）
[]į||||||||[]įğ
ş· · ·**，\!!!!!!!!!!!!!|-!ț¢
ſąjįſi
ſiji
!bjjjj±SĒ
į№.
ſaeºſ
&##
ļīĒ
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CLINTON GROUP.
No. 4.—No. 14, page 69.
Fucoides gracilis, H. One of the most persistent and common fossils of the group.
No. 5. – No. 15, page 70 of Report.
Figs. 1, 2 and 3. Pentamerus oblongus. I. The large variety, somewhat three-lobed. 2. A
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
5
more circular form of the same shell. 3. A side view of a specimen intermedi-
ate in form to the other two. Rochester.
Cast of upper valve of same fossil.
. Cast of lower valve.
Delthyris brachynota, H. Reynolds's Basin, Niagara county.
No. 6. —No. 16, page 71.
Orthis circulis, H. Two views — a beautiful striated circular shell, with a very
small area. Reynolds's Basin, Niagara county.
. Atrypa congesta, C. (Jour. Acad. Nat. Sci. Vol. 8, page 265, plate 16, fig. 18.) Shell
striated concentrically, and not with radiating lines as the figure would indicate.
. Atrypa naviformis, H. A nearly smooth shell, somewhat concentrically striated, and
with a few more prominent lines of growth. (Compare Atrypa linguifera — Si-
lurian Researches, pl. 13, fig. 8.) Sodus Point.
. Atrypa plicatula, H. A small plicated shell, with three of the folds raised in front.
Reynolds's Basin, Niagara county.
. Crinoidal joint, natural size and magnified. A widely distributed fossil, being known
abundantly in New-York and Ohio.
ORGANIC REMAINS OF THE CLINTON GROUP.
|
|-
|
|
|
į
|
!
|
'''W
|
|
|
|
|
|
|
fh
|
|
|
|
|
|
|
|
|
|
|-
|
|
E.---
ſì
|
||-
|
|
|
±
|
�
|N
�
�
|
|-
šº:№！！. . ſ
|}
N|
�
|
|×
|
|
-Ź2źã=№zī:：:£§
•-，@?<！！！∞-ğ）======::=?=~：: ---- №¿š§
ź，ã-§§）;§
źā$№.3，?zº.§¶· • •'№š§§
。2}}}\，}$§§·?? - ¿ $ŠŇ
ājº)ſ（$§§№šŞSN
22%-№ș،\\
??№
&9}
™N
�§§Ņ*-- （-，+，-，-，-，-， º
ſä§\\\\\\\\\\\}\\-✉º
ſae§§\\\\\\\\\\\\\\\\§§
ÊSSN\\\\\\\\\
----Ņ-æ：№sēšș№
Ř™Ā，ae-№šſ§§§）
Kae//////////)])/ № №
*№é，// ±
%%¿? Ē&&¿{。?�ſºº、。 --?
--№
„egéājēĒĢš§§§
¿№;
„æÊĒĒĢ
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CLINTON GROUP.
No. 7. –No. 17, page 72. -
*
Fig. 1. Orthonata curta, H.
Fig. 2. Nucula macharaformis, H.
Fig. 3. Cypricardia obsoleta, H.
Fig. 4. Nucula mactræformis, H.
Fig. 5. Avicula leptonota, H. Shale of the Wolcott ore bed in Wayne county.
Fig. 6. Cypricardia? angusta, H.
Fig. 7. Lingula elliptica, H.
Fig. 8. L. oblata, H.
Fig. 9. L. acutirostra, H. /
No. 8. —No. 18, page 76.
Fig. 1. Strophomena elegantula, H. Shell with elevated ribs and fine striae between. It bears
a considerable analogy to S. sericea and S. transversalis, but is quite distinct
from either. Sodus Point. -
Fig. 2. Strophomena corrugata, C. (Jour. Acad. Nat. Science, Vol. 8, p. 256, pl. 14, fig. 8.)
Rochester.
Fig. 3. S. cornuta, H. A small neatly striated shell, armed with small rigid spines on the
hinge line. Sodus Point.
Fig. 4. Atrypa hemispherica, (Silurian Researches, pl. 20, fig. 7.) Abundant in the green
shale at Rochester.
Fig. 5. Littorina cancellata, H. Young shell. Sodus Point.
Fig. 6. — * “ Old shell, with the markings worn off.
Fig. 7. Posidonia? alata, H. Green shale, Rochester.
Fig. 8 and 8 a. Atrypa affinis & Old and young shells. Sodus Point.
Fig. 9. Calymene 2 trisulcata, H. A small trilobite, with three furrows on each side of the
middle lobe of the head. Rochester.
Fig. 10, Agnostus latus. Green shale, Rochester.
Fig. 11. Tentaculites minutus.
Fig. 12. Graptolites Clintonensis. An abundant form in the upper green shale of the group.
Sodus Point. -
No. 9. —No. 19, page 77.
Fig. 1. Fucoides biloba, VANUxEM (Geological Report, page 79).
Fig. 2. Tail of Hemicrypturus. & 4 ( (.
Fig. 3. Smooth crinoidal joint. & 4 { %
Fig. 4. Lingula oblonga, C. (Annual Geol. Report, page 65.)
L. Clintoni, WANUxEM (Report, page 78).
Fig. 5. Strophomena depressa. (Leptana depressa, Dalman.)
ORGANIC REMAINS OF THE CLINTON GROUP.
No. 7.
º
! º …
º,
išº'º'
§§§%
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 10. – No. 33, page 101.
Fig. 1. Asaphus limulurus, GREEN (Monograph, p. 48). Resembles and is perhaps identical
with the A. longicaudatus of Murchison, and holds the same place in the series.
-- Lockport. -
Fig. 2. Head of A. limulurus. This portion of the fossil is abundant at Rochester.
Fig. 3. Calymene Niagarensis, H. Abundant at Lockport. Closely resembles in many
respects the Calymene senaria of the Trenton limestone.
Fig. 4. Bumastis barriensis, (Silurian Researches, p. 656, pl. 7 bis, fig. 3, a, b, c and d ; pl.
14, fig. 7, a and b.) The specimen figured is nearly twice the usual size, though
there is one in the State collection one-third larger than the figure. Lockport.
No. 11. – No. 34, page 103.
Homalonotus delphinocephalus. (Silurian Researches, pl. 7 bis, fig. 1 a, 1 b.) Trimerus
delphinocephalus, GREEN (Monograph, fig. 1, p. 82). This trilobite often attains
the length of seven or eight inches, and very rarely twelve inches. Lockport.
ſº
s.ſ. tº ： · ***
×
‘II ‘ON
。āſā， №aeae
§§、、、。
ĢĢae
№ſſae
№， №-
ĢĒĒĢ№Ē
§§§§§§§§§§）;№
§§§§§§§。
§№ĒĒĒĒĒĒĒĒĒ№•
º№ĒĒĒĒĒĒĒ№aeae:Exae×
¿№ĒĒĒĒĒĒĒĖĖ№Ē:：:::：
¿=== E FÆ№=--~~~~ 5ĢĒ，
*: < :*：IĘĚ3?$$$];！,’:’, :,:≡
±±（−3）}）; ** *
--> +， ·） --- - -… * * *
* * * =：=≡≡-， º į
• ！=*= *• → •*,…）,
№ſĢĒ
:：=≡:#№ĒĢĒ#
“diſh OHS) WłI W3)WINI (IHL HO SNIWIWIGI*I OINWł)?HO
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE NIAGARA GROUP,
No. 19.
Fig. 1. Platynotus Boltoni, CoNRAD, Annual Reports. (Paradovides Boltoni, Bigsby. GREEN,
Monograph, p. 60). This is one of the most rare and beautiful of the trilobites
in the Niagara group. Lockport.
Fig. 2. Bumastis barriensis. Specimen of the ordinary size. Lockport.
Fig. 3. Asaphus coryphaeus. (Jour. Acad. Nat. Sci. Vol. 8, page 277, pl. 16, fig. 15). Lock-
port.
9
§§
º
- # § § º
º § § § § r § §
º ---------º-
§
§§
*
§§§
§ §
§ §§ º
º:
º
§
§
º º
º
sº
º #
§ § &
sº º
§ §
;
§ §
* º § g
§ §§ §
§§§
§
- §§ §
º
§§
§
§
tº:
§
§§§
§§§
§º.
§
§§§
§
§§§º
§
§
º §§
} ł § §
§§
sº
#:
§§
*: : §§§
ºś &: º
§
§ º ; jº. º:
§
--> º sº
§ º º
º
º º
§
ºšič *:
; § §§ - tºº
º ſº -* --- - º
§
- §§§ º; -
§ ; -
§
§
§
§
º º
§ - §: - § §
§§ § &: ºš
- º: º; §
3. §§§ Sºtº ſ: §§ §:
ºft - £ºš.
-- " - §º
§§§
§
- : Fº
§§
§§§
§
§ § § §
§§ ----
§ º
º º
3
§
.***
§ § *
§§ § §
º * º & & c. º
º º § §
§: . º: --
§:
ºś
ºś
§§ ;
Yºs § §:
§§§
§
º
Ž
º
§§§
;
&
§§§
gzº
§§
§
§ º :
§§§º
*.* § : º §
§§ ºf ºle
§
§: § § § t
§
§ §
§§§
§§ tº
§ §
§
; §
. º
- § ºś
* f
º
§
**.sgºy
º
§
tºº
§§§
* §
§§
º
i
$. ...?.S.A./2////.5' (X)/?) ('0///S'.
/////S//$ A /l/ / ///VS/S' .
Li TH OF H. N. DiC O ſ? .
GEOLOGY OF THE FOURTH DISTRICT.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 12. — No. 35, page 104 of Report.
1. Strophomena subplana, C. (Jour. Acad. Nat. Sci., vol 8, page 258.) Lockport.
2. Strophomena depressa, Productus depressus, M. C. t. 459. (Leptana depressa, DAL-
MAN. Swedish Transactions, p. 106, t. 1, f. 2; HISINGER, Petrefacta Suecica,
p. 69, t. 20, f. 3. MURCHIson, Silurian Researches, p. 623, pl. 12, f. 2.) An
abundant fossil in the shale of the Niagara group. Lockport.
3. Strophomena striata, H. Common at Rochester and Lockport.
4. Strophomena transversalis. (Leptaena transversalis, DALM. l. c. p. 109, t. 1, f. 4;
HIS, Pet, Suec. p. 69, t. 20, f. 5. Silurian Researches, p. 629, pl. 13, f. 2.)
No. 13.-No. 36, page 105 of Report.
1. Delthyris Niagarensis, CoNRAD (Jour. Acad. Nat. Sci. vol. 8, p. 261). Lockport.
2 and 2 b, Delthyris radiatus. (Spiriſer radiatus, M. C. t. 493. Silurian Researches, p.
624, pl. 13, f. 6.) Lockport. -
3 and 3 b. Delthyris staminea, H. (References, Spirifer crispus 2 Silurian Researches,
p. 624, pl. 13, f. 8. Delthyris crispa, DALM. l. c. p. 122, t. 3, f. 6; HIs. Pet.
Suec. p. 73, t. 21, f. 5). Lockport.
4 and 4 a. Delthyris decemplicata, H. Lockport; and Delthyris sinuatus. (Terebratula
sinuata, SoweRBy in Linn. Trans. Vol. 12, p. 516, t. 28, f. 5 and 6. Delthyris
cardiospermiformis, HIs. Anteckn. Wol. 4, t. 7, f. 6. DALM. sur les Terebratules,
p. 124, t. 3, f. 7. HIs. Pet. Suec. p. 74, t. 21, f. 9. Spirifer cardiospermiformis,
Von BUCH sur les Spirifers et Orthis, t. 1, f. 7. Spirifer sinuatus, Silurian
Researches, p. 630, pl. 13, f. 10.) Wolcott.
5. Orthis flabellulum (a) & (Silurian Researches, pl. 21, f. 8. O. callactis DALMAN.)
Lockport.
6. Orthis canalis, (Silurian Researches, p. 630, pl. 13, f. 12, a ; also pl. 20, f. 8. Orthis
elegantula 2 DALMAN. Von BUCH sur les Spirifers et Orthis, pl. ii, f. 3, 4 and 5.)
Sweden, Monroe county. - -
7, a, b, c. Orthis hybrida. (Silurian Researches, pl. 13, f. 11.) Sweden, Monroe county.
No. 14— in part No. 37, page 108.
1. Atrypa imbricata. (Terebratula imbricata, Silurian System, p. 624.)
2. Atrypa. (Species undetermined.) Lockport.
3, 4 and 4 a. Atrypa cuneata. (Terebratula cuneata, DALMAN. HISINGER. Silurian Re-
searches, p. 625, pl. 12, f. 13.) -
5. Atrypa nitida, H. A very abundant species, but usually more or less distorted.
Lockport.
6. Atrypa affinis, (Terebratula affinis. M. C. t. 324, f. 2. A. reticularis, DALMAN,
HISINGER, &c.)
11
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 11.
s
s
º
º§§Š
% º * * | W
% ſº | . W
tºº
*ś
%|º Šº
3 * * * *
ſº
sº $'S$2.
% | §§
§
§ sº-ºº:
§§
ŞS:
§§
gº/M
ſº W º
&|\º
še:
33
ºšº º
12
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 15.-No. 38, page 108.
Fig. 1. Orbicula? squamaeformis, H. Sweden, Monroe county. (Reference, Silurian Re-
searches, p. 625, pl. 12, fig. 14 a.) .
Fig. 2. Lingula lamellata, H. Lockport.
Fig. 3. Orbicula corrugata, H. Rochester.
Fig. 4. Avicula emacerata, CONRAD (Jour. Acad. Nat. Sci, vol. 8, p. 241, pl. 12, f. 15).
No. 16. — No. 39, page 109.
Figs. 1 and 2. Euomphalus hemisphericus, H. Rochester.
Fig. 3. Cornulites arcuatus, CoNRAD (Jour. Acad. Nat. Sci. vol. 8, p. 276, pl. 17, f. 8),
No. 17. —No. 40, page 110.
Fig. 1. Orthoceras annulatum ? (Reference O. annulatum, M. C. t. 133, Silurian Re-
searches, pl. 9, f. 5.) .
Fig. 2. Conularia quadrisulcata, MILLER (M. C. t. 260, f. 3 and 4; HIs. Pet. Suec. p. 30,
t. 10, f. 5; Silurian Researches, p. 626, pl. 12, f. 22). Lockport.
13
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 14.
º
N;3-6%
U
§§§ . * s
wº
S
:§
§
§
º
14
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 17.-No. 41, page 111.
Fig. 1 and 2. Caryocrinus ornatus, SAY (Jour. Acad. Nat. Sci. vol. 4, p. 289). Lockport.
Fig. 3. Cyathocrinites pyriformis, (Silurian Researches, p. 672, pl. 17, f. 6. Ichthyocrinus
lavis, CoNRAD Jour. Acad. Nat. Sci. vol. 8, p. 279, pl. 15, f. 16.)
No. 18. —No. 41 (read 41 bis), page 113.
Fig. 1. Hypanthocrinites calatus, H. Lockport.
Fig. 2. Hypanthocrinites decorus. (Silurian Researches, p. 672, pl. 17, f. 3.) Lockport.
Broken off at the base of the arms.
Tig. 3. Hypanthocrinites decorus. Lockport.
Fig. 4 and 5. Marsupiocrinites? dactylus, H. Lockport.
ORGANIC REMAINS OF THE NIAGARA GROUP.
i. § WA º
ºlº
| º
% º | | ! \\
sº
| †† |
*
W. Wºº
|
º
#:
|
|
|
|
:
;
;
|
º
\ *ºss %
*sº
%
º
ºft
| º º º
§ §§ | º
ºliº
* | # %
º º
†
ºil;
ºf
ſº
º §
la
16.
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 19.
Fig. 4. Caryocrinus ornatus.
Figs. 5 and 6. Interior structure of the plates.
Fig. 7. Part of a plate enlarged, showing the pores which communicate with the external
surface.
No. 20.
Fig. 1. Anatomical structure of the Caryocrinus ornatus.
Fig. 2, Arrangement of the capital plates, showing the mouth composed of several conical
plates.
No. 21.
Fig. 4. Cyathocrinus 2
Fig. 4 a. Anatomical structure of the same fossil.
Fig. 5 a. b. Cyathocrinus? These two species have not been determined.
17
ORGANIC REMAINS OF THE NIAGARA
GROUP.
º
º
|
º
§ |
º
& §
ſ
No. 20.
No. 21.
flºº
º
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 22.
Fig. 1. Catenipora escharoides, LAMARCK. (For synonymes and references, see Silurian
Researches, page 685.) Very abundant and widely distributed. The upper part
of the Niagara limestone.
Fig. 2. Catenipora agglomerata, H. A very distinct species from the last. Abundant at a
single locality in Ogden, Monroe county.
Fig. 3. Porites º
Fig. 4. The same fossil, mostly removed, leaving only the lines indicating the stages of
growth. (See pages 86 and 91 of Report.)
19
ORGANIC REMAINS OF THE NIAGARA GROUP.
.* No. 22.
§
§
N
N
§
\\
*
\
s
i
§: *.
§
§
§
§
§
ºº
WSº
20
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE NIAGARA GROUP.
No. 23. — No. 42, page 115.
Fig. 1. Gorgonia? reteformis, H. Lockport.
Fig. 2. Gorgonia Ž ? These two are fossils in the shale at Lockport.
No. 24. —No. 43, page 116.
! This fossil, though very beautiful in its appearance, is obscure, and for want
of time has not been decided. Lockport. *
Figs. 2 and 3. A coral resembling Isis. … Lockport,
Fig. 1.
21
ORGANIC REMAINS OF THE NIAGARA GROUP.
º
|
|||| º
ºilº
* |
|
|
|
|
|
|
|
!
\
|
|
|
|º
º
| º º
%. º
|
|
N
|
|
|
|
|
º
|
|
|} | º §.
iº §tº
º
º;
|jj; |
§ujiii;
ji
|lli, l
º
\
|
|
|
|
|
|
W
º
§ º
* ºl
§§
*
| |
l | º | º |
º
ºil
& ºl
|. º | Lºli
| \||
º º | | |
ºli, º : § § º {
ſh ºl; º º t | #| ||
º º § \\ | -
: § º
§ Prº º §
º | º: º
* º
§ º
^ ſº
§ | º
º * t | | i. |
; ºil
ºil
§§§
ºilſ
§§§§
.*.*. º ſº º | ºil II, |
§
§§ }
º
till º
| |liº;
º: [. º;
\
\
ſºliº;
i. | § g j
º: º
\
\
Wºlff,
#Tº | º \º
|||| - °, #!/??,
|
tº: | |. - - H ## # #! jº º gº
| | % º W #|| | | | || º # #| #
| | | - 4. | "... f. | . . i º - d Fº
º | * . . . . \\\|| III:H. º
& & * NNW NM i. | W. || || º 4 º' *
|:/ſº sºlſ|| ||||||ſº |,
º \ºwlſº #// “N
ºlº Ali)\\ | &Nº.
ºlºl (MAW;h W\\\\\\ §Wºlffº g as S
ºf MW) | |\\\ilºſº/º S
º
º |
in lili | \\
º 0.
§li j º:
** as sº § |ºliº º
º
|
|
º
|
d
ºu WHill||W - §§§ Wº% º
º: l º Jº W | | |||}|† By | º ? % S
| #º | º }} | |/|| | º % *
Wºº {||||||}}}/\\\\\ 5
º s º ſº . . . \\
§
l
Alſº
Ş.
º
Nº|| ||
ºš)
sº º Y {}
y
|
º
seasº
º
%
º
-:
22
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE ONONDAGA SALT GROUP
No. 25. —No. 54, page 137.
. Cornulites, n. s.
. Orthoceras lave, H.
Loaconema Boydii, H.
. EuOmphalus sulcatus, H.
Fig. 5. Delthyris 2
Fig. 6. Atrypa 2
Fig. 7. Avicula triquetra, H.
Fig.
Fig.
Fig.
Fig.
:
These all occur at a single locality, and but one other shell has been seen in the group.
Two of these species are not satisfactorily ascertained.
ORGANIC REMAINS OF THE WATERLIME GROUP.
No. 26. — No. 58, page 142.
Fig. 1. Delthyris plicatus. Orthis plicatus, (Geol. Report Third District.)
Fig. 2. Avicula rugosa, CoNRAD (Annual Reports).
Fig. 3. Tentaculites ornatus. (See Silurian Researches, p. 628, pl. 12, f. 25.)
Fig. 4. Littorina antiqua, CoNRAD (Annual Reports).
Fig. 5. Atrypa sulcata, VANUXEM (Geol. Report).
Fig. 6. Cytherina alta, CoNRAD (Annual Reports).
ORGANIC REMAINS OF THE PENTAMERUS LIMESTONE.
- No. 27. — No. 25, Report of the Third District, page 117.
Fig. 1. Pentamerus galeatus. Atrypa galeata, DALM.
Fig. 2. Euomphalus profundus, CoNRAD (Annual Geol. Report).
Fig. 3. Atrypa lacunosa 2 This fossil is considered by Mr. Conrad as identical with the
Terebratula lacunosa of Europe.
Fig. 4. Lepocrinites Gebhardii. The stems, one covered by a thick calcareous coating, and
the other showing the rings.
ORGANIC REMAINS OF THE I)|ELTHY RIS SHALY LIMESTONE.
- No. 28.-No. 27, Report of Third District, page 122.
Fig. 1, Strophomena punctilifera, CoNRAD.
Fig. 2. Strophomena radiata, CoNRAD. These fossils occur in the Delthyris shaly limestone
in central New-York, but at the west the S. punctilifera holds a higher position.
23
ORGANIC REMAINS OF THE ONONDAGA SALT GROUP, etc.
No. 25.
|
|
aſſiſ|| |hſ
||||||
|
º
|
|
|
|
|
|
|
|
|
|
|
|
|
|
|
|
|
|
|
º
º
|
|
|
||
i
|
|
|
|
ill
|#
º U. º
iſſ
24
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE ORISKANY SANDSTONE.
No. 29.-No. 59, page 148.
Fig. 1. Delthyris arenosa, CoNRAD (Geol. Annual Report, 1839, p. 65).
Fig. 2. Atrypa elongata, CoNRAD (Annual Report, 1839, p. 65).
Fig. 3, Atrypa peculiaris, CoNRAD (Annual Report of 1841).
No. 30. – No. 60, page 149.
Fig. 4. Atrypa unguiformis, CoNRAD. (Hipparionya proacimus, VANUXEM, Geol. Report, p.
124, fig. 4.)
Fig. 5. Cast of Delthyris arenosa.
The fossils of this rock are scarcely found in the Fourth District, except in loose scattered
masses which are common in Seneca county. The rock is abundantly fossili-
ferous on the eastern shore of Cayuga lake.
25
ſº
\！
%
ſ
§
| º
. &
/
&S ...
§
sº
\\
ſ/
º
w
W
ºs（ae***
（№s
wº
º-S- - F----
:E:E: E-- Tº -
sº-º-º-º-º: -> x- S-3
|};
}vių!į}}
\-\,||
\\\\\\\\\）|ſ}}
∞ √{
~§
====
- £:=
sº
º
*:::::::::::::
º:
°{{NOJ SCINWS XNW XISI?HO GHHJ, „HO SNIWIŃGI?， OINVÉ)}{O
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE ONONDAGA LIMESTONE.
No. 31. — No. 61, page 157.
Figs. 1 and 1 a. Favosites alveolaris.” Williamsville, Erie county.
Fig. 2. Favosites gothlandica. Williamsville.
Fig. 2 a. — G-mº A single tube magnified twice, and presenting a double row
of pores upon the side.
^
Fig. 2 b. A fragment from a honeycomb specimen, showing the transverse lamellae. Wil-
liamsville. -
Figs, 3, 3 a, and 3 b. Fragments of crinoidal columns, showing the pentapetalous canal-and
crenulated edges of the plates, etc. Williamsville.
No. 32. — No. 62, page 159.
Fig. 1. Favosites fibrosa? Clarence, Erie county.
Fig. 2. Astrea rugosa, H. Le Roy.
—ms
* For synonymes and references of the genus Favosites, see Silurian Researches, pp. 681, 682 and 683; also GoLDFuss,
Petrefacta, Genus Calamopora.
27
ORGANIC REMAINS OF THE ONONDAGA LIMESTONE.
ſae
|
ſſſſſſſſſſ,
№ſ （¿?
(±§！！！！！！！！！！！！！！！！！！！ :） … :（ :） ::：:::-:
±
|-----~--~~~~، ، ،~~~•№:！-！－-*********（
∞== s … :-）: ''， – . . --&g.
–
CY)
GĒĒ№±！======
Z-•
§3 ---+--ż
===A s īīīīīīīīīīīīīīīīī
Ē№ºº! ¡¡¡¡¡iſ
ſiſſae
;ſ&#ff
ſae;，，№rſ=***« %
ſyyſſºşț¢;&&ſ，ſa ſa， º， ſ.º. e
ſſſſſſſſſſsaeyaeº，
¿¿?ſaevĀĂĂȚĂTOER
¿ā.¿ae§;}^^^Y®Ä׺
：*~--~{
}}ķffffffffff;ţ###ģț######{}ÄģÄÄ
+●¿}
ĢYNA,È˧§
}}∞ §§§§§ģ\º$ſſſſſſſſſſſſſſſſſſſſſ
¿
țģ#############ğģ→
Ë
№ºrs)
±ffwaſ āºae
∞ √∞ √gg
ſaeſ?
§
§
§§
ŠS
§§
Ņ
Ņ
Ž
º
ſº
º
lº
Ø
Ø
ſº
º
7%
ſº
V)\,
ſj;$ſ;
%šși
%%%%）
2%%%%%
№， º
ºſº
ſº
(ſ
ſº
jº
º
§§
ſºſº
ſº
§
§ w
º
wº
§
(ſ
%
W
W
S
•№º）~~
§ żae
§Ņ'.
SŅs
§，21
º
%.
\º
*
º
º
sº
º
%%aer.
£%--
Źź
4&،
�A™È2%，
∞$ -46%2222€.
ſºsŅſae±，±，±，±，±
GNQÈYºg
* ，ºx.%Ø%2€.
%
SNŠ.§：
±√：Źź
$s：
````3.
§§§§§§§::：
§:§©®-
§§§
§§§\!\!\，
ĢÈ\\
¿ŠŅ\\\\{\\
-¿?·№È\\{\\
Ñ\\
Ñ
§ŠSĒŅ
§S
§`N
∞ √≠ √¶§§
S★S™）§§
§¶√∞
SSSī£®©
№№S?
2№¿№ſſae
22，2€！！！！
-ſae¿.*¿¿.*：
-·æ：（~š -， …..！
S-（+） *（）_<！， SS （№º！！！ ！！
§§se■■■S™:
<！--*æs****§×3№
§§§§§§：№
§：№ſ
&&！S=№
£§！®£§！！！！！！！！！S
ſaesºxaeaeaeae***--ſae！！！
22，2€<£®
±，±，±，±，±，±，±，±，±），¿?，
28
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE ONONDAGA LIMESTONE.
No. 33. —No. 63, page 160.
Fig. 1. Cyathophyllum — ? Caledonia.
Fig. 2. Cyathophyllum dianthus, (GoLDFUss Petrefacta, p. 54, pl. 15, fig. 13, and pl. 16, fig.
1. Silurian Researches, p. 690, pl. 16, f. 12, 12 a to 12 e.) Caledonia. -
Fig. 3. Syringopora ? The fossil is silicified, standing in relief upon the surface of the
rock.
No. 34.—No. 3, page 132, Report of the Third District.
Fig. 1. Pentamerus elongata.
Fig. 2. Hipparionya (Atrypa) consimilaris.
Fig. 3. Delthyris undulatus.
These fossils are not common in the Fourth District, though they have been seen at two or
three localities.
29
ORGANIC REMAINS OF THE ONONDAGA LIMESTONE,
No. 33.
*º-sºº."
E:--ºº: a-s:
-º- ºr-.
Aſºº º: Wiji=
| * * {i : | º ſ
|iº §
&e
ſºlº
º
lº º
jº
º
ºf:
!ºli
tº ". . . tº c.
|. § º' lº
||||||||
| º,
º * I. -
|
º
º
º
§'s §§§
| | ſ º li º
\ // % §.
º $º
|jº - §§
º |º
ºftº j %
jkºff}
% ſº ºf
º
d | | jī
| H. |||}|†
W | |
º
º
Wºjſij}|
º Miſſ i É
- | º
º #º
§ººl §§
... • º * tº: % º
º
\\
\
: *
§§ § º º
§ º º
3
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CORNIFEROUS LIMESTONE,
No. 35.-No. 67, page 171.
Fig. 1. Atrypa scitula, H. Williamsville, Erie county.
Fig. 2. Paracyclas elliptica, H. Shell very closely resembling a Cyclas. Le Roy, Genesee
county. *
Fig. 3. Strophomena acutiradiata, H. Near Buffalo.
Fig. 4. Strophomana crenistria, H. Vienna, Ontario county.
Fig. 5. Delthyris duodenaria, H. Five miles east of Buffalo.
Figs. 6 and 6 a. Pleurorhyncus trigonalis, H. Williamsville.
No. 36 — No. 68, page 172.
Fig. 1. Pterinea 2 cardiiformis, H. Clarence Hollow. -
Fig. 2. Tentaculites scalaris, SCHLoTHEIM (Silurian Researches, p. 643, pl. 19, f. 16).
Fig. 3. Orthonychia A new genus, from its resemblance to a claw or talon. There
are several other species. Williamsville.
Fig. 4. Euomphalus? rotundus, H. Clarence Hollow.
Fig. 5. Calymene crassimarginata, H. A common and widely distributed fossil of this lime-
stone. Williamsville.
Fig. 6. Acroculia erecta, H. Williamsville.
31
ORGANIC REMAINS OF THE CORNIFEROUS LIMESTONE.
No. 35.
wº
sº
- e."”
**
*
<>
mň
º § - £:
| # º: - § º
ſº iſ ºf º:
{ \;
§ | \; |
f .
\
º
º
º º º
§§ \
º
º
\ \\
|
º
|
§ }
§
||||||||||}|\\\\\\\\\\\\\\ §
| M - - §º - .
|||||||||}|\\\\\\\\\\\\º
; |\\\\\\\\\\\\\\\\\\\º sº-
§ Wº § º º
\\\\\\\\\\\?\\\\\\\\\\
Wº \\
| º \\\\\\\\\\\\\\:
º Wº:
- }|| |||\º
iſ lº
º
| º
º
| | ||
: ºº º: % f || ||
;:/7.% % § |||}}}}}||
Aft: %2/º:
ºf ºf º
%. º º -
% ſ/ſºft
y A. gº
º & º
; % Ž º º | - d
& A º ſº § || || º
* º ! º
§ ºğl
º %
% ſº }} º
A. -
§
º
º
r º
º % -
w d
§. ºf # ſ ſ -
*. ...'ſ Hºſº |
- ºf lºſſ. º
“g º! ºil. º
| #
#º
|
--- ſ
§ſ. | -
º, ºf
º
*satīþi
*#sº
º ºs; R
º
Sº
h; º
32
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CORNIFEROUS LIMESTONE.
No. 37. –No. 69, page 174.
Fig. 1. Ichthyodorulite. Undetermined. Victor, Ontario county.
No. 38. – No. 70, page 175. -
Fig. 1. Odontocephalus selenurus, CoNRAD. (Asaphus selenurus, EATON. Calymene odonto-
cephala, GREEN.)
Fig. 2. Cyrtoceras undulatum, WANUxEM (Geol Report).
Fig. 3. Strophomena undulata, W. (Geol. Report).
Fig. 4. Orthis lentiformis, W. (Geol. Report).
Fig. 5. Atrypa prisca.
Figs. 6 and 7. Ichthyodorulite, and section of the same.
Fig. 8. Strophomena lineata, CoNRAD (Annual Reports).
The fossils of this illustration, with the exception of 3, 5 and 8, are not as abundant in this
rock in the Fourth District, as those preceding.
33
ORGANIC REMAINS OF THE CORNIFERöUS LIMESTONE.
No. 37.
#s:sis:s:#S$
$$$$. #S$ºs.
še *śs
ſº |
º
t?
wº
- JMrs. Ba'daſes Čez.
*
No. 38.
Willº
ºilij
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE MARCELLUS SHALE
No. 39. —No. 71, page 180.
Fig. 1. Orthoceras subulatum, H. Bloomfield, Ontario county.
Fig. 2. Strophomena setigera, H. Avon, Livingston county.
Fig. 3. Strophomena mucronata, H. Avon.
Fig. 4. Strophomena pustulosa, H. Avon.
Fig. 5. Avicula muricata, H. Avon.
Fig. 6. Avicula lavis, H. Avon.
Fig. 7. Avicula equilatera, H. Bloomfield, Ontario county.
Fig. 8. Orthis nucleus, H. Avon.
Fig. 9. Orbicula minuta, H. Avon.
Fig. 10, Tentaculites fissurella, H. Avon,
Fig. 11. Atrypa limitaris, Orthis limitaris, VANUxEM (Geol. Report). Le Roy, Genesee
COunty.
ORGANIC REMAINS OF THE HAMILTON GROUP.
No. 40.-No. 78, page 196.
Fig. 1. Bellerophon patulus, H. Kidder's ferry, Cayuga lake.
Fig. 2. Microdon bellastriata, CoNRAD (Jour. Acad. Nat. Sci. Wol. 8, p. 247, pl. 13, fig. 12).
Fig. 3. Cucullea opima, H. Seneca lake shore.
Fig. 4. Nucula? oblonga. Seneca lake shore.
Fig. 5. Nucula lineata ? PHILLIPs (Palaeozoic fossils, p. 39, pl. 18, fig. 64). Cayuga lake
shore. - -
Fig. 6. Tellina? ovata, H. Seneca lake shore.
Fig. 7. Nucula bellatula, H. Ogden's ferry, Cayuga lake.
Fig. 8. Cypricardia truncata. (Cypricardites truncata, CoNRAD, Jour. Acad. Nat. Sci. Vol. 8,
p. 244, pl. 12, fig. 17. See Geol. Yorkshire, pl. fig, )
Fig. 9. Modiola concentrica, H. (See Modiola semisulcata, Silurian researches, pl. 8, fig 6.)
No. 41. —No. 79, page 198.
Fig. 1. Turbo lineatus, H. Ovid, Seneca lake shore.
Figs. 2 and 3. Delthyris mucronata, CoNRAD (Annual Report of New-York Geol. Survey,
1841, p. 54). Eighteen-mile creek.
Fig. 4. Atrypa prisca. (Terebratula affinis, M. C. t. . T. prisca, Won BUCH; T. reti-
cularis, BRowN, Lethea Geognostica. Atrypa reticularis, DALMAN. A. affinis,
Silurian Researches.) Eighteen-mile creek.
Fig. 5. Atrypa concentrica, BROWN (Lethea Geog.). Eighteen-mile creek.
35
REMAINS OF THE MARCELLUs SHALE AND
ORGANIC
No. 39.
%iºğ
§§§
|
º &
º
gº
ºmmºn y
§ºrº
º Rººs
filliliği
º
º
º
wº
|
HAMILTON GROUP.
{-3.
ź
º
|
i
º
3.
\\
%iº
º
§
%||l\\
iº
%|
* * * * * * * *
36
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE HAMILTON GROUP.
No. 42, — No. 80, page 200.
Fig. 1 and 1 a. Atrypa spinosa, H. Specimens from Eighteen-mile creek, with the spines
removed.
Fig. 1 b. A portion showing the imbricated lamellae and concentric elevated lines.
Fig. 2.
Fig. 3.
Fig. 4.
Fig.
Fig.
Fig.
Fig.
Fig. 1.
Fig. 2.
:
Atrypa spinosa, with the spines partially visible. Moscow.
Atrypa concinna, H. Moscow. -
Strophomena inequistriata, CoNRAD (Jour. Acad. Nat. Sci. Vol. 8, p. 254, pl. 14, f.
2). Moscow. A.
Delthyris zigzag, H. Moscow.
. Calymene bufo, GREEN (Monograph, p. 41). Moscow.
. Cryphaeus calliteles, GREEN. Moscow.
. Loa onema nea'ilis, PHILLIPs (Palaeozoic fossils, p. 99, pl. 38, fig. 183. Terebra nea-
ilis, Sow BRBy in Geol. Trans. 2nd series, Vol. 5, pl. 54, fig. 17). Seneca lake
shore. *
No. 43. —No. 81, page 202.
Avicula orbiculata, H. Eighteen-mile creek.
Atrypa rostrata, H. Eighteen-mile creek.
Figs. 3, 4 and 5. Undetermined species of Atrypa. Eighteen-mile creek.
Fig. 6.
Delthyris sculptilis, H. Eighteen-mile creek.
No. 44.—No. 82, page 203.
Figs. 1 and 2. Avicula decussata, H. 1. A cast in limestone. 2. The shell preserved in
shale.
37
ORGANIC REMAINS OF THE HAMILTON GROUP.
No. 42.
s:-y ºr
º ſº &
\ \ §
:*. # º º ſº
º §: º
º §3. sº
º g
º 3. %2Xº,
W º ſº º §
& §
N &
º
\\
\\
38
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE HAMILTON GROUP.
No. 45.-No.84, page 205.
Fig. 1. Dipleura Dekayi (head), GREEN (Monograph, p. 79).
Fig 2. Orthonota undulata, CoNRAD (Annual Geol. Reports).
Fig. 3. Delthyris mucronata, CoNRAD (Annual Reports). This is the common form of this
fossil in the sandy shale of Eastern and Central New-York; at the west it is less
elongated and more rotund. See figs. 2 and 3 of No. 41.
No. 46.-No. 86, page 208.
Figs. 8, 8 a. and 8 b. Delthyris medialis, H. Moscow.
Figs. 9 and 9 a. Two views of a young shell of the same species as the above. Moscow.
Fig. 10. Delthyris fimbriata, CoNRAD (Jour. Acad. Nat. Sci. Vol. 8, p. 263).
Fig. 10 a. Cast of the upper valve of the same fossil.
Fig. 10 b. A small portion of the shell magnified. Moscow.
39
ORGANIC REMAINS OF THE HAMILTON GROUP.
§
No. 46.
%lºws
| tº
º
- - zº % %
ğ% /
40
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE HAMILTON GROUP.
No. 47. – No. 85, page 207.
Fig. 1. Delthyris granulifera.
Fig. 1 a. End view of the same, showing the spiral coil within the shell. Pavilion, Genesee
county.
Fig. 1 b. A specimen with a more extended hinge line. Moscow.
Figs. 1 c and 1 d. A younger shell of the same species. Pavilion.
Figs. 2 and 2 a. Delthyris congesta, H. Seneca lake shore.
Fig. 3. Delthyris mucronata, H. View of the hinge.
Fig. 3 a. Area of lower valve.
Fig. 3 b. Lower valve. Moscow.
41
ORGANIC REMAINS OF THE HAMILTON GROUP.
\
No. 47.
!
g
i
º
- ſº º
º
ğ º º
|
| ſº
;
# |
% § | º
%iº
8 ºr tº
º
% %
GEOLOGY OF THE FOURTH DISTRICT.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
5.
1.
2 and 2 a. Strombodes
ORGANIC REMAINS OF THE HAMILTON GROUP.
No. 48.-No. 87, page
. Cystiphyllum cylindricum, with Aulopora tuba formis attached. (Lonsdal.E in Silu-
rian Researches, p. 691, pl. 16 bis, f. 3, 3 a and 3 b.)
. Cystiphyllum id., a smaller specimen, with the bases of crinoidal columns attached.
Eighteen-mile creek.
Strombodes helianthoides 2 (PHIL. Palaeozoic fossils, p. 11, pl. 5. f. 13. Cyatho-
phyllum helianthoidum, GoLDFUss, Petrefacta, pl. 20, f. 2.) York, Livingston
county.
Strombodes distortus, H. Moscow.
Strombodes? rectus, H. Moscow.
…”
. Strombodes simplea º H. This fossil resembles the S. plicatum, but is apparently
distinct.
No. 49.
Cyathophyllum (Strombodes 2) turbinatum ? (GoLDFUss, p. 56, pl. 16, fig. 8.) York,
Livingston county.
? A young individual.' York.
3 and 3 a. Cyathophyllum — ? A rare but strongly marked species. Moscow.
43
ORGANIC REMAINS OF THE HAMILTON GROUP.
No. 48.
,
wº
|. ºz º
|| ||
sº
º
º gº §
\\ º
§
º
§ ~ | º, W. |
§ § \ % º
§W. %
- W |
- §
§
§ § ºfºº # Zºº. . .
sº SS W º Wilſº £2. -
§ º -% %
%
Îift § tº gº #ſ
#|| % §
º
| º º
º
* . . . . º
º ſº
º w ſtſ * . . . .
§§ |ff
§§ | :
§
§§
sº
§.§§
§§
sº
}{S \
§§§
Sºś
§§§
*}% ſ%
Fº §§ º
º º
º |
Ağ
† § º
º º
º
§ - º:
º
5.
# §
No. 49.
44
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE TULLY LIMESTONE.
A.
No. 50. — No. 92, page 215.
Fig. 1. Atrypa cuboides 2 (Reference, SoweRBY, Geol. Trans. 2d series, Vol. 5, pl. 56, f. 24,
PHILLIPs, Palaeozoic fossils, page 84, pl. 34, f. 150. Pages 215 and 216 of
Report.) - .
Fig. 2. Orthis resupinata. (PHILLIPs, Palaeozoic fossils, p. 67, pl. 27, f. 115. Spirifera
resupinata of the same author; Geol. of Yorkshire. Terebratula resupinata,
Sow. Min. Conch. t.325. Anomites resupinatus, MARTIN. Orthis Tulliensis,
Report of Third District, page 163.)
Fig. 3. Atrypa lentiformis, WANUXEM (Geol. Report, page 165).
Fig. 4. Atrypa affinis. (For synonymes and references, see page 198 of this report.) This
fossil is partially a cast, with the shell remaining on the edges which are com-
pressed. -
Fig. 5. Atrypa cuboides 2
ORGANIC REMAINS OF THE GENESEE SLATE.
* No. 51. — No. 94 and 95, pages 222 and 223.
Figs. 1 and 2. Avicula fragilis, H. -
Fig. 3. Strophomena setigera. See fossils of the Marcellus shale.
Fig. 4. Tentaculites fissurella. See fossils of the Marcellus shale.
Fig. 5. Lingula spatulata.
Fig. 6. Lingula concentrica.
Fig. 7. Atrypa quadricostata. -
Fig. 8. Orbicula lodensis. The four last figures are from the Report of the Third District.
45
ORGANIC REMAINS OF THE TULLY LIMESTONE.
*.*;;+.*;，
§@₪
∞:'，
¿№sſae)
§：№§§§
aeſºſ
4%
FEASE, $83,
- -
*::FE:
5-
*
* -º-º:
… .
º
sº º
Zºº,
º
*
:=3
E.-:
s:--><
-:
-->
W.
E-->
ºš
22
. . . . . . . . . ;
Ä
ſae
}●ſae
№ºae
46
GEOLOGY OF THE FOURTH DISTRICT,
ORGANIC REMAINS OF THE PORTAGE GROUP.
No. 52. — No. 104, page 241.
Fucoides graphica. Flagstones of Gardeau.
No. 53. – No. 105, page 242.
Fucoides verticalis. Sandstone of Portage.
47
ORGANIC REMAINS OF THE PORTAGE GROUP.
EE||
z-e-
- s:=> E}
* ==#EE ź.
#EEE?
=s=s===E==
==#º
Sºss- ====
º-º-º-º:
- #ssf:===
sº->3
ºs----es: º
:
º-º-º:
º
Cº-º-º-º-º- v
--~~~ º
ºſ º- -zºº
2
3 2
ºš2%
º:
ÉSE=SE;
º- S$s:sº- º -
E
==||ÉS=#=;
Sèss==
º
*s-se
º º #º
-->
ºffl
\;=s . . . . ºfflº º
*=$:==#####
e-ses
ſ *:::=
|
º
tº
º º §
SS § ; :
#.
º:
§§§
º
§
§
§§
f
|
|
W- º§.
\ºW
-! dº
%%§
āşşş
- Fºssº,'.... S
§§
§
SS
š
º
º:
48
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE PORTAGE GROUP.
No. 54. — No. 106, page 243.
Fig. 1 and 1 a. Avicula speciosa, H. Cashaqua shale, on Cashaqua creek,
Fig. 2.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
i
Ungulina suborbicularis, H. Cashaqua creek. -
Bellerophon eaſpansus 2 (Silurian researches, pl. 5, fig. 37.) Cashaqua creek,
Orthoceras aciculum, H. Cashaqua creek. ~
Clymenia? complanata, H. Cashaqua creek.
Goniatites sinuosus, H. Cashaqua creek.
. Pinnopsis acutirostra, H. Cashaqua creek.
Pinnopsis ornatus, H. Cashaqua creek.
No. 55. —No. 107, page 245.
Fig. 1 and 1 a. Delthyris lavis, H. Western shore of Cayuga lake.
Fig.
Fig.
Fig.
Fig.
Fig.
Fig.
i
Fig. 8.
Fig. 9.
Cardium? vetustum, H. Shore of Lake Erie.
Orthis tenuistriata, H. Crooked lake shore.
Lucina? retusa, H. Lake Erie shore, in Chautauque county.
Nucula lineolata, H. Occurs with the last.
Astarte subtextilis, H. With the last. -
Bellerophon striatus BRONN. (PHILLIPs, Palaeozoic fossils, pl. 40, f. 198.) With
the last on Lake Erie shore. - -"
Goniatites bicostatus, H. Chautauque county.
Goniatites sinuosus, H. As above, fig. 6. Chautauque county.
49
ORGANIC REMAINS OF THE PORTAGE GROUP.
§§
№È§È
§ÈŞ
§§
§
§ÈŠŅ
-£};
ķ#·
-ſae
ģ
ģý%
¿
%
、。
ģff
@
%%;
§
N
）
Ä\
ì
š
§:
sº
º-º
º-º-º:
sº-ºº:
gºš
{{\\}\\}
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE PORTAGE GROUP.
No. 56. – No. 108, page 247.
Fig. 1. Cyathocrinus ornatissimus, H.
Figs. 2, 3, 4 and 5. Portions of the column at different distances from the base. Lake Erie
shore, Chautauque county.
51
ORGANIC REMAINs of THE PORTAGE GROUP.
s
º
§
;
º\
§
º
|
º
;
|
9.
º
º
:
;
NW
|
H
º
§
5.
º
:
i
No. 56.
rºl
gº
1. º § Ş & &
ºğ
§§§
*Sºf ~
(Čš º
!. º & ºš º
º § §§
W
Nº.
}x
i
§
|
gº
º
º
i
º
i
§
l
t
|N
\E.
g
º
s
W
§
}
N
N: § §§
§§
\iš
\\ - º Sº W
,' Nj
º
º
º
sº
* ..." wº º
º 32
* * * º
* : ****
... .ºlº &
tº "... º.
º, ºxº
ſº
&
**** º
º: &
; : * ºf ſº
º
sº- lº
º
*...*
ºlk,
º
*
ºriº
ºf:
º
sº
G wº
&
ſ º
tº:
|
&
§
\\
\\
N
N
|
sº lº
$º Y
º-ºº:
º WN
52
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CHEMUNG GROUP.
No. 57. — No. 116, page 262.
Fig. 1. Calymene nupera, H. (Reference C. laevis, PHIL. Palaeozoic fossils, pl. 55, fig. 250.)
No. 58. —No. 117, page 262.
Figs. 1 and 2. Avicula pecteniformis, H. Lower and upper valve. An abundant fossil of the
Chemung group. i
Fig. 3. Avicula longispina, H. Painted-Post.
Fig. 4. Avicula spinigera, CoNRAD (Jour. Acad. Nat. Sci. Vol. 8, p. 237, pl. 12, fig. 3.)
Painted-Post.
No. 59.-No. 118, page 263.
Fig. 1 a and b. Avicula damnoniensis, (SoweRBY, in Geol. Trans. 2d series, Vol. 5, pl. 53,
fig. 22. PHILLIPs, Palaeozoic fossils, pl. 23, figs. 90, 91 and 92.)
53
ORGANIC REMAINS OF THE CHEMUNG GROUP,
No. 57.
No. 58.
§§§
§
>†< º sº NYX.3%
à% §§§
㺠º *. *ś §§§
ſº % §§§
%|}}} §§7% §§
% jä º
§§§
sº §§
E-3 sº
\ ſi
§ §§
§: 33%;
§§ É%§} - §t
ºº:
iº
§
§
iW
§º§W
§§Š
§
$:
% W
Ø % \ §§
> º §
šāºft\{\\
§§ - % % | º \
N º *ºº |
Sºº-º-º-º-º-º: %
|
%
% º
N
ſ
&
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CHEMUNG GROUP.
*:
No. 60,—No. 119, page 264,
Fig. 1. Pterinea? suborbicularis, H. Hobbieville, Allegany county.
Fig. 2. Pecten duplicatus, H. Phillipsburgh, Allegany county.
Fig. 3. Lima rugaestriata, H. Rockville, Allegany county.
Fig. 4. Pecten cancellatus, H. Phillipsburgh.
Fig. 5. Avicula? signata, H. Rockville.
Fig. 6. Pecten ? convexus, H. Rockville.
Fig. 7. Pecten striatus, H. Painted-Post.
Fig. 8. Pecten? crenulatus, H. Rockville.
Fig. 9. Pecten? dolabriformis, H. Rockville.
Fig. 10. Lima glaber, H. Phillipsburgh.
Fig. 11. Lima’ obsoleta, H. Phillipsburgh.
No. 61. –No. 120, page 266.
Fig. 1, Strophomena nervosa, H.
Fig. 1 a. An enlarged portion of the shell. Campbelltown, Steuben county.
Fig. 2. Strophomena bifurcata, H. Napoli, Cattaraugus county.
Fig. 3. Strophomena arctostriata, H. Hobbieville, Allegany county.
Fig. 4. Strophomena pectinacea. Hobbieville.
Fig. 5 a, b, c. Strophomena interstrialis, Orthis interstrialis and Leptana interstrialis.
(PHILLIPs, Palaeozoic fossils, pages 61 and 216, pl. 25, fig. 103.) 5 a. Inner side
of a flat valve. Chemung. 5 a. A magnified portion of the shell, 5 b. The two
valves somewhat compressed. Ithaca. 5 c. The convex valve with the shell
partially removed. Elmira. \
.**
- No. 62. – No. 121, page 267.
Figs. 1 and 1 a. Orthis carinata, H. Painted-Post.
Fig. 2. Orthis impressa, H. Near Elmira.
Figs. 3 and 4. Orthis interlineata, (SoweRBy in Geol. Trans. 2d series, Vol. 5, pl. 54, fig.
14. PHILLIPs, Palaeozoic fossils, p. 63, pl. 26, f. 106.)
Fig. 5. Orthis unguiculus, Atrypa unguiculus, (SoweRBY in Geol. Trans. 2d series, Vol. 5,
pl. 54, fig. 8. Spirifera unguiculus, Pal. fossils, pl. 26, f. 119.)
Fig. 5 a. A cast from Bald Hill, near Ithaca.
Fig. 5 b. Lower valve, broad variety. Dexterville, Chautauque county.
Fig. 5 c. Upper valve. Painted-Post.
Fig. 5 d. Fragment of brownish sandstone, filled with casts of the shell. Jasper, Steuben
county. 55
ORGANIC REMAINS OF THE CHEMUNG GROUP.
~~~~:）, …?≡≡≡ºvº， ºſ
∞ſaeae •
№
§
º
|
i.
**********șae
§
f §
|
#
****
#
§§*
ſęſt;!！！!!
șįjį
&&
§§
§§§§§§§§
·§ģ
&&§$%§§
$§§
§§§¿$ſ
§§
§§§
§§
™Ę§§
£=№
ëșēšēj
§:№
çº，
ſãğźģě~
ſae¿
¿?
。•。
-№g！
No. 62.
ºniº
a tº
ſ
lºº
Hº
ſ
gº
iii.
lºſ
º
ſ
Fº
~。}}
¿¿$àË
§§§§§§
§§§Ř$ÈëÈ
§§§§§§§A SS
șţÈ
§§§§
~≡
׿(）
ģ
¿
56
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CHEMUNG GROUP.
No. 63. — No. 122, page 269.
Figs. 1 and 1 a. Delthyris mesastrialis, H. Cayuta creek.
Fig. 2, Delthyris mesacostalis, H. Angelica. r
Fig. 3. Delthyris disjuncta ? PHILLIPs (Palaeozoic fossils, pl. 29, fig. 128, f. g. h., and 129,
pl. 30, fig. 129). Chemung.
No. 64. — No. 123, page 270.
Fig. 1. Delthyris cuspidata, H. This fossil resembles some of the varieties of Spirifera
disjuncta. (SoweRBY, Geol. Trans. 2d series, Vol. 5, pl. 54, figs. 12, 13; pl. 55,
fig. 2; also Pal. fossils as quoted above.) Cayuta creek.
Fig. 2. Delthyris acanthota, H. Upper and lower valves. Chemung.
Fig. 3. Delthyris mucronata ? (See fossils of Hamilton group.) This is the only specimen
resembling this fossil seen in the Chemung group.
Figs. 4 and 4 a. Delthyris inermis, H. Twenty-mile creek, Chautauque county.
Fig. 5. Delthyris acuminata, H. 5 and 5 a. Internal casts of the shell. 5 b. Enlarged
portion of a cast of the external surface. Ithaca.
57
ORGANIC REMAINS OF THE CHEMUNG GROUP.
Eº
58
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CHEMUNG GROUP.
No. 65. —No. 124, page 271. -
Fig. 1 and 1 a. Atrypa dumosa, H. 1 b, Cast of the same. Chemung and Elmira.
Fig. 2. Atrypa hystria, H. Bath, Steuben county.
Fig. 3 and 3 a. Atrypa tribulis, H. 3 b. Cast of the same. Ithaca and Chemung.
Fig. 4. Atrypa 2 tenuilineata, H. Cattaraugus county.
No. 66.
Fig. 1 a, b, c, d. Atrypa laticostata, Terebratula laticostata. PHILLIPs (Palaeozoic fossils,
p. 85, pl. 34, fig. 153). These are all apparently varieties of the same shell, and
referable to this species.
Fig. 2. Atrypa laticostata, var. 2 This species has six ribs distinctly elevated in front, while
the other varieties have usually but three ribs elevated. It is probably a distinct
species. - -
Fig. 3. Atrypa. (Species undetermined.) Greenwood, Steuben county.
Fig. 3 a. Atrypa contracta, H. About three ribs elevated in front. Shell contracted. Green-
- wood, Steuben county. . *
Fig. 4, 4 a and 4 b. Atrypa eaſimia, H. This is an abundant form at Ithaca; often associ-
ated in great numbers, but rarely with any other fossil.
Fig 5. Atrypa polita, H. A very neat shell, with the lower valve much elevated in front.
Jasper, Steuben county.
No. 67.
Fig. 1, 1 a, and 1 b. Atrypa mesacostalis, H. Shell with from four to six strong ribs along
the mesial elevation and depression of either valve, while they become obsolete
toward the margins. The casts are very common everywhere. Ithaca, Che-
mung, &c.
Fig. 2, 2 a, and 2 b. Atrypa duplicata, H. Shell with two ribs elevated in front, and two
on each side the mesial fold. Dexterville, Chautauque county.
59
ORGANIC REMAINS OF THE CHEMUNG GROUP.
S$º
*
s
1.
b
i
N
N
§
§
Y
Q aftº
º
Nº
§
§
|
§
\
W §
|\
|
|\\
wº
§
º
§
§§§
§§
§
º:
%||
º
| º
º sº
(ſ
§
|
ſ
%
iº
}
j ſ
º
º
%
º
%
%
|
f
º
l
º
60
GEOLOGY OF THE FOURTH DISTRICT,
*
ORGANIC REMAINS OF THE CHEMUNG GROUP.
No. 68.-No. 125, and part of 127, pages 273 and 275.
Fig. 1. Filicites? An abundant fossil at Ithaca and other places in Tompkins county.
Fig. 2. Sigillaria Chemungensis, H. One-half the natural size. Elmira.
61
ORGANIC REMAINS OF THE CHEMUNG GROUP.
！！！！！！！！！！！ :-） . . . （-ae-） → :）！！！！！！！！！！！!！！！！-№ssae
，，... :（. . . ::： ~ ¡ ¿！:--:- - - -， -.---3，5±5， ±š§§！！！！！！！$. （3！！）;№sae
！！！！！！！; （3），…...…（№s. №ºÆ， *■■■■ ■-№：№-№ſſaeğ№.،
„…， ... （:-（-a）∈， √≠ √æ√≠№º-， * .*º№: ， ,--*、、” ș5）<C)
******* ！！ ！！！！！！！！！！！！！！！$，?...º №3，№. ！！ ）-≡-----*№.№s ae
∞:'，''））; lae！ №. ！！----Fº-rº~-*-…--~--~■■■.ae
， -€， ºſ ≡≡:£§！！！… :（**）:--~~---№ ~~~~）.：&& ！$$（）
， ！-，::：&aeºſ， š:■ ■■■* -ae， …！№ ：-----§§§§§
º·∞
\
; :º o: W
W § º
º
WNWA\\\ \\\\\\?
- sº N - \\ \ § \\
"Wºº
\ Nº. .. º W. º
º º t |
- \\\ W tº º
No. 68.
º ： · · · ·：·ººg,
：，
gaeae
|\，¿ºſ ſae。ffffffffffffff（J)j)/ff//////zzzzzzzzzzzparn-„aevaeſſ
\！â№È\āÈ™Ē%ź@%%%%%%%%ſae%
º.%
ſ.ſ.
ſae.
|
）
ſae-
\\
R
}
7/
N
∞
：ſae：
U %%22。ź}}|
ŅŅ ∞
%//
WįN№§§ſae/%%%%%%%%%2%%%%%%%%%%%%%%%%%%%%%%%Ø3
&#žĂſ@%：：=
%ae
}،
Ēģ%：%%ae2ź%Źź
- GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE CHEMUNG GROUP.
No 69.-No. 127, page 275.
Fig. 1. Sphenopteris law.us, H. Pine valley. This is the only specimen of this fossil yet
observed. f
63
organic REMAINS OF THE CHEMUNG GROUP.
No. 69.
º
º § Fº º t WWM
ſº | º º | º | \
i
W
W
|
º|
\
W
\
|
|
|
!
§|
N
.SNº:
t§º
i:
i
W
|
W
}
\
|
:}
i
º
:
º
|
{ b.
|
|
|
|
|
|
|
||
|
º ſ
#}
º
|
G {{º}} ź.
| º
sº
E. º º
º &
|É
É%|||}º ºf;
#}}{{}}|º ſº
g º: º !
g
§ § §
% ºš jW.
% ºš §
\.
#º
ſ
:
§
|§
\\à
º
|;
§
º |
º!º
|º º
: \º º
àº. º º |\ º º º
º º * i |
sº
ºft;
º
º
º sº
º
ſ
§ º
º|ffſ W º *
'% sº
|
º
º
º
:
º
º
f |
§ \\
º
'º º
U º' |. º
{\\
•= \
\º
º
ſ
§ſ ſºM&
~§
.|
)N
%Sº
º
s
º}}
§
s
º
º
ºº§
|
|
\
d :-ºQ
§º
º
º
§§
º
|
|ſº
#w |
.º!º
º|
º
§§
|
N
º:
|º
º
\d
º
|
\
W
§
!
ſ
|
-|
||
|
|
|t
|ſº-:}º:
§§3.
|º3.º
ººº33-
#.§ſ§;[.º
|º§--º
||ºiW ºlg-:i
|ºg
-lººi:|
§ºº|
}§
|
64
GEOLOGY OF THE FOURTH DISTRICT.
ORGANIC REMAINS OF THE OLD REDSANDSTONE.
No. 70,—No. 130, page 281.
Fig. 1. Scale of Sauripteris Taylori, H.
Fig. 2. Scale of Holoptychus nobilissimus, AGAss. (Silurian Researches, plate 2 bis, figs. 1,
2, 3, 4, 8 and 9). -
Fig. 3. A smaller scale of Holoptychus 2
Fig. 4. A fragment of a tooth waterworn before being imbedded.
No. 71. –No. 131, page 282.
Jaw-bone and teeth of Holoptychus. -
For further illustration of the fossils of the Old red sandstone, see plate 3 of this report.
- No. 72. –Page 186.
Cypricardia Ž angustata. Report of Third District.
ORGANIC REMAINS OF THE CONGLOMERATE.
No. 73. — No. 139, page 291.
Fig. 1. Euomphalus depressus, H. (Reference E. serpens, PHIL. Pal. Fossils, pl. 36, fig.
172.)
Figs. 2 and 3. Cypricardia rshombea, H.
Fig. 4. Cypricardia contracta, H.
These fossils are all from a single locality in Chautauque county, and the only place where
I have seen fossils in the conglomerate. -
65
ORGANIC REMAINS OF THE OLD REDSANDSTONE, etc.
No. 70.
W
y
§
\\
§
º
º
• * . . . . .” %;º
%
% º
Ž
%
%gº --> #:#
- e:E: -. - :=====ãº:ãºgºź.:#º
===
ºz; ºft
%
-- => Egº º
º::====<=
%
%
& §§ § º
%
r #º
#}\%.º.
\%.º % §§§§§ %;º:
% % t º } gº
* * * * * * B. %)
%\ºj% % º://
ſº
% º ſº º º {} & ńs -
§ tº º
º º º fº º %
º ſ ..
% %
}
ºff;
/
A. % Ø
# jià t # º ºs §§ |jºjº
;#ff § - ºft ſ ######### | |ſ
%ft. %| jº |W/
66
º
3
ESE
Eğ: ººº-ºº::= HS:
Ssº:55:5:3
ºts. ES:S-st
º
sº-
º
E:
É
É
*
s: #3: £º
====3:=33°
ºº:::::::::::::: ===º
:::::::::: £º
É *
% º
%
%
%
- - CLINTON GROUP.
Illustrations No. 7 and 8, transposed.
NIAGARA GROUP.
No. 11 is repeated at the head of the page over Strophomena. The numbers in this one and the five following ones
should be made to correspond with those on the opposite pages, viz. 12, 13, 14, 15, 16, 17. - *
In the names and references for No. 13, Delthyris sinuatus, with its synonymes, follows in the same line with Delthyris
decemplicata; this should commence the line below, preceded by fig. 8.
CORNIFEROUS LIMESTONE. W
In the illustration No. 38, fig.8 is accidentally removed from Strophomena lineata (See page 175 of this Report;
z’ GENESEE SLATE.
Illustration 51: the numbering of fossils, after 4, should be 5, 6, 7, 8 (See page 223 of Report).
CHEMUNG GROUP,
Illustration 59, fig. 2, Avicula acanthoptera, name omitted,
A P P E N DIX.
( A• )
/
Ridge Road of Lake Ontario.
The elevations given of the Ridge Road bordering Lake Ontario, shows no important variations
within the limits of the Fourth District. Since that portion of the Report passed through the press, I
have had an opportunity of examining a continuation of the same, or another similar ridge, in the
northern part of Oswego and the Southern part of Jefferson counties, and about six or eight miles
distant from the shore of Lake Ontario. This ridge is about four hundred feet higher than the lake,
but having been traced only for a few miles, it is impossible to say whether it continues at a uniform
elevation. I am aware that this discrepancy in the elevations between this portion and that in the
western part of the State, has been urged as an objection to the supposed mode of its production, 1
consider, however, that the existence of such a ridge, with all the attendant phenomena before noticed,
is paramount to every objection regarding its mode of formation; and different elevations of different
portions do not in the least impair the force of the conclusion.
In the example before us, it offers a fact in proof that the lake was not quietly drained by the
reduction of the barrier at its outlet, but that the change has taken place by an elevation of the land.
The varying elevation of the ridge proves that the amount of upheaval was greatest towards the north-
east, in the region of a nucleus of hypogene rocks, and that it gradually subsided towards the South-
west, where the strata become undisturbed.
It is not improbable, however, that further investigations will prove the existence of a series of
parallel ridges in New-York, showing the effects of successive elevations, aided likewise by a reduction
of the outlet.
The different elevations of the well marked Tertiary deposits, upon the valley of Champlain and
the St. Lawrence, as well as those upon the New England coast, become interesting in connexion with
this subject; and, as before suggested, it is not improbable that future investigations will prove the eleva-
tions of these deposits, and the production of the lake ridges, to be synchronous, at least to a certain
extent. Still it is very probable that some of the more elevated ridges may have emerged before any of
the marine tertiary appeared above the level of the Ocean.
[GEOL, 4th DIST.] 83
662 : APPENDIX,
( B, )
Ridge Road of Lake Erie.
I have been furnished, by the Hon. G. W. Patterson, of Westfield, Chautauque county, with the
following elevations of the Ridge road extending along Lake Erie. The elevation of the Ridge road,
where crossed by the New-York and Erie railroad, is one hundred and ninety feet above Lake Erie.
At Westfield village, the elevation is one hundred and eighty-seven feet above Lake Erie, showing a
difference of three feet between these two points, distant about fifteen miles. Mr. Patterson thinks that
one hundred and ninety feet may be considered about the average elevation.
( C. ) -
Modern action of rivers in deepening their channels,
Under this head, many important facts have been omitted; and from some recent observations, I am
satisfied that the operation of the present streams is far more effectual in deepening their channels, than
even the most Sanguine supporters of the power of existing causes would advocate.
Since this Report has passed through the press, I have had an opportunity of examining the Lebanon.
reservoir, in Madison county, (constructed for supplying the Chenango canal,) which, during the month
of April, 1843, broke through the dam, and passing down a ravine, joined the Chenango valley.
The surface occupied by this reservoir was about ninety acres, with an average depth of about
twenty-five feet. The dam at the outlet is of gravel, built very strong, and flagged upon the inner side
with stones. During the thawing of the snow, the reservoir became filled; and the wasteweir being
defective, it soon commenced undermining it, and the whole was removed in about an hour. The
water then excavated a channel to the bottom of the dam, about thirty feet deep, through which it flowed
off rapidly into a broad valley below. The force of the water here appears to have been inconsiderable;
the materials of the dam lie spread over the bottom of the valley very uniformly, and the trees are still
standing as before. About one quarter of a mile below the dam, the valley contracts, and the small
stream flows in a gravelly channel with steep sloping banks. It is here that we first perceive the effects
of this moving body of water, in uprooting and breaking the largest trees. These falling across the
channel, formed with the earth and shrubs, temporary dams, until the accumulating force of the water
carried all before it, prostrating hundreds of the largest trees. The gorge gradually narrows, and its bed
and banks become rocky. These have been swept clean for many rods, where before they were covered
with gravel and clay. For about a quarter of a mile before opening into the valley of the Chenango, the
banks are of rock, and from thirty to fifty feet high. Between these banks, in a channel of fifty or
sixty feet wide, this body of water bore its accumulated detritus, trees and timber. From the great
pressure, owing in part to obstructions by the formation of temporary dams, the channel was both
widened and deepened. Persons living in the vicinity, have estimated that the channel for a considerable
APPENDIX. 663
distance was excavated to the depth of six feet. Two or three small falls along the stream have
receded several rods, and huge fragments in immense numbers were torn from the sides of the ravine.
The whole of this accumulated mass of earth and stones was forced out from the mouth of this ravine
into the level valley of the Chenango; and after the water subsided, an extent of fifteen acres was found
completely covered to the depth of from one to five or six feet. The thin-bedded sandstone from the bed
and banks of the ravine lies in slabs of two to four feet in length and breadth. Boulders of limestone,
sandstone and other northern rocks, are confusedly intermixed with the other materials. One of the
boulders of limestone lying near the centre of this area of fifteen acres, I estimated from measurement
to weigh about eight tons, and there were numerous smaller ones, and others of the Oriskany sandstone
of three or four tons. The uprooted trees, and the timber of two mills which were destroyed in the
course of the stream, were scattered over an extent of fifty acres. The passage of this body of water
through the ravine occupied four or five hours, and nothing could exceed the grandeur of its resistless
force. - \
What has here resulted from an artificial dam, may easily happen from natural causes. Many
of our ravines open into broader valleys above, and a great body of Snow melting in this situation and
pressing toward the outlet, would carry forward any prostrate trees; these accumulating in some narrow
passage would form a temporary dam, which, when broken away by the increasing pressure, would
add new materials to form a stronger one at the next narrow pass. In this way the same scenes may be
enacted as in the case just described, and the bed of a ravine or stream may be deepened several feet
in a few hours. -
The process here described, with others before mentioned, operating through ages, is sufficient to pro-
duce the deep ravines which we now find, though the quantity of water flowing in them may never have
been much greater than at present. The actual amount of excavation produced in this way is immense,
and I am perfectly satisfied that the same causes have always operated from the incipient stages of these
deep gorges to their present condition. In favorable situations, large and comparatively permanent lakes
may have been thus formed, and their subsequent bursting produced the phenomena attributed to lakes
originally remaining on the higher ground. -
( D. )
Elevation of Lakes.
The following memorandum of the elevation of some of the smaller lakes was mislaid at the time that
chapter passed through the press. These elevations were furnished by Mr. Healy, an engineer on the
New-York and Erie railroad. -
FEET. -
Bear lake summit. . . . . . . . . . . . . . . . . . . . 755.4 above Lake Erie.
Cattarauguslake summit. . . . . . . . . . . . . . . 725.5 (£ {{
Mud lake. . . . . . . . . . . * @ 9 º' e º 6 e º e g º e º 'º 833. 7 {{ &
Cassadaga lake . . . . . . . . . . . . . . . . . . . . . . 725.0 {{ {{
Leavenworth summit, between the valley of -
the Little Connewango, in Randolph, and
the Allegany. . . . . . . . . . . . . . . . . . . . . 859 {{ {{
664 APPENDIx.
. ( E. )
Elevation and depression of water in the Great Lakes.
For numerousinteresting facts in relation to this subject, see an article in the 16th volume of Silliman's
Journal, by Gen. H. A. S. Dearborn. - -
See also a pamphlet on the same subject by Edward Giddings of Lockport.
( F. )
Salines.
In the course of this Report, several unimportant Salines were mentioned as occurring in the higher
groups of the system. One of these was at Jefferson, and another near Big-stream point. As they ap-
peared to offer no inducements for further exploration, they have merely received the attention which was
considered due to them. Since this Report has passed through the press, I have learned that salt in con-
siderable quantity has been made from a similar spring in Dundee, Yates county. Not having visited
the place, I am unable to say what probability there is of a supply of brine; and in the absence of any
definite information on the subject, this notice is all that can be given. -
( G. )
Among the persons who have written upon subjects connected with the Geology of Western New-
York, I have been able to name the following. Some of these have not been alluded to in the Report.
DR. BIGSBY on the Geology of Genesee county. American Journal of Science and Arts, Vol. 2, p. 250.
SAY on the Fossils of New-York. ID. Vol. 1, p. 384; Vol. 2, p. 34.
EATON on the Geology of the Salt springs. ID. Vol.6, p. 242. - -
EATON on the Geology of the District along the Erie canal. ID. Vol. 8, p. 195, and Vol. 13, p. 383,
GEDDEs on the Geology of Ontario valley. ID. Vol. 11, p. 213. -
EATON on Diluvial deposits. ID. Vol. 12, p. 17. **,
J. VAN RENsseLAER, Remains of the Mastodon in Ontario county. ID. Vol. 12, p. 381.
DEARBORN on the variations in the level of the lakes. ID. Vol. 16, p. 79.
Carburetted hydrogen at Fredonia. ID. Vol. 17, p. 398.
THOMAS on Diluvial scratches and furrows. ID. Vol. 17, p. 408.
WADsworth on the Geology of the Genesee river. ID. Vol. 18, p. 209.
Buffalo Mineral Spring, Analysis of, by C. U. SHEPHERD. ID. Vol. 20, p. 156.
SILLIMAN on an Oil spring in Allegany county. ID. Vol. 23, p. 97.
Rogers on the Falls of Niagara. ID Vol.27, p. 326.
HAYEs on the Geology and Topography of Western New-York. ID. Vol. 35, No. 1.
Say on the Crinoidea. Journal of the Academy of Natural Science of Philadelphia, Vol. 4, p. 289.
BIGSBy on a Trilobite at Lockport. ID. Vol. 4, p. 765. -
CoNRAD on the Fossils of New-York. ID. Vol. 8, p. 235.
HAYEs on the Inflammable springs in Ontario county. New-York Medical and Physical Journal, Vol. 3, p. 49.
HENRy’s Topographical Sketch of New-York. Transactions of the Albany Institute, Vol. 1, p. 87.
GEDDEs, Observations on the Geological features of the south side of the Ontario valley. ID. Vol. 1, p. 55.
HARLAN on the Eurypteris lacustris. Transactions of the Geological Society of Pennsylvania, Vol. 1, p. 98.
EATON's Canal Rocks, and his communications to Silliman's Journal. - - -
A chapter upon the Agriculture of the District had been prepared for this work, as mentioned in the
text; but since this department was subsequently committed to Dr. Emmons, it has been omitted as un-
necessary, a separate report on the subject being in preparation. --
- INDEX,
As
Aboriginal names, pages 146, 219, 225, 406.
Absence of an acknowledged basis at the west, and difficul-
ties arising therefrom, 513.
Accretions, 41, 42.
Achmite, 99.
Acid springs, 134, 464.
Acroculia, 172.
Action of freezing water in deepening river channels, 375.
Action of the ocean upon rocky shores, 322.
Agassiz, Prof., his theory, 330.
Agnostus latus, 72; its lowest position, 74.
Agricultural characters of the soil overlying the Medina
sandstone, 45; Niagara group, 99; Onondaga-salt group,
136; Corniferous limestone, 170; Marcellus shale, 179;
Hamilton group, 195, 210; Portage group, 239; Chemung
group, 260.
Aikin, Prof., survey of Coal district in Maryland, 23.
Akron, Ohio, rocks at, 502.
Alexander, J. H. Esq. and Prof. Ducatel, geological and
topographical survey of Maryland, 23.
Allegany county, surface, rocks, elevation, etc. 484.
Alluvium, 472, 489.
Alumina, sulphate, 98, 260.
American stag, 365.
Analogy between the Hamilton group and shale of the Nia-
gara group, 185.
Ancient condition of the continent during the transport of
boulders, 337; and during the formation of terraces, 352,
Ancient valley of the Genesee, now filled with drift, 372.
Anculotus, 397.
Angular and unworn boulders, 333.
Anhydrite, 98.
Anthracite coal, its lowest position, 28.
Anticlimal axis in Western Ohio, extent and effects of, 513.
Apulia, shale near, 184.
Argillaceous iron ore, see Iron ore.
Asaphus, 101.
Astarte, 245.
Astrea, 159.
Atrypa, 29, 71, 72. 108, 137, 142, 148, 149, 171, 175, 180,
198, 200, 202, 215, 216, 222, 255, 271, 276, 456, 462,
467, 472, 485.
Avicula, 29, 30, 76, 108, 137, 142, 180, 202, 203, 222, 229,
243, 255, 256, 262, 263, 264, 46ſ, 465, 473, 481, 486, 494.
Avon sulphur springs, 313.
[GEOL. 4th DIST.]
84
1B,
Baryta, sulphate, 44, 65, 67, 141, 179, 194, 214, 221, 239.
Bayfield, Capt., his observations on the St. Lawrence, 335.
Bays or ponds of Lake Ontario, 55, 417.
Beaches and sandbars, removal of, 409.
Beaches, observations on ancient, 353.
Beaches, modern, and lake ridges, 354.
Bear lake, 407.
Beck, Dr. L. C. & A. Eaton, agricultural survey of Rems-
selaer county, 6.
Beck, Dr. T. R. & A. Eaton, agricultural survey of Albany
county, 6.
Bellerophon, 29, 48, 196, 229, 243, 245.
Birdseye limestone, 28.
Bitumen, 177, 221, 257, 310.
Bituminous limestone, 84, 85; sandstone, 310, 485.
Black micaceous shale, 248, 485.
Black-river limestone group (Birdseye and Chazy), 28; its
extent in New-York, Canada, Kentucky, Pennsylvania
and Virginia, 28.
Black-Rock, 140.
Black shale, 177; slate, 218 ; varieties of slaty shale, 230,
Blende, 460,
Blocks of Medina sandstone on Niagara limestone, 340.
Bloody brook, gorge of, 398.
Blue fluid in concretions of Genesee slate and Marcellus
shale, 221.
Blue limestone of Ohio, &c., identity with the Hudson-river
group of New-York, 503, 504.
Bog and argillaceous iron, 419.
Bog iron ore, 140, 437, 447, 470, 491.
Bones and scales of fishes in the Old Red sandstone, 280.
Booth, Prof. W. C., geological survey of Delaware, 23.
Boring for coal, 239; for brine, 45, 135, 417.
Boulders, 319, 320; position and mode of transport of the
northern, 332; means of transportation, 334; northern, not
found in intertropical regions, 333; angular and rounded,
333; rare in the higher groups, 333; position of the for-
mation in relation to the ancient drift, 339.
Boulders in Wayne county, 416; in Monroe county, 424;
in Orleans, 437; in Niagara, 443; in Seneca, 453; in
Cattaraugus, 491; of iron ore, 491; used for burning to
lime, 496.
Brachiopoda, 229.
Briggs, Prof. C., report on the geology of Ohio, 23.
*.
666 INDEX,
Brine springs of the Medina sandstone, 34; of the Onondaga-
salt group, 134 – 136; origin of the latter, 135.
Brine, borings for, 45, 135, 417.
Broken and drifted shells, 63, 64. N
Brown spar, 92, 98.
Buffington's well, 311.
Building and flagging stones, 62, 84, 87, 88, 130, 154, 156,
162, 163, 164, 215, 421, 432, 438, 447-8, 451-2-3, 456,
460, 463,471-2-3, 477-8, 481, 485-6, 488, 492, 494, 497.
Bumastis, 29, 101.
Burning springs, see Carburetted hydrogen.
G,
Cacholong, 67.
Calcareous matter, increase of in a westerly direction, 515.
Calcareous tufa, see Tufa ; marl, see Marl; spar, see Car-
bonate of lime.
Calciferous sandrock, 28, 317.
Calciferous slate, 80, 117.
Caledonia spring, 170,
Calymene, 29, 30, 72, 101, 172, 200, 262, 462, 472.
Cambrian system, equivalents in New-York, 20.
Cameroceras, 29.
Canada, 27.
Canadice lake, 407.
Canandaigua lake, 407.
Camoga spring, 170, 308.
Carbonaceous shale, 84.
Carbonate of iron replacing fossils, 260; of lime, see Lime.
Carbonic acid gas in water, 428. *-*
Carboniferous limestone, 19, 179, 411, 508.
Carboniferous system, 19, 284.
Carburetted hydrogen, 309, 418, 491, 497, 498.
Cardium, 245.
Carnelian, 67.
Caryocrinus, 111.
Cashaqua shale, 218, 224, 226, 463, 467, 473.
Cassadaga lake, 407.
Casts of shrinkage cracks, 230; of flowing mud, 232, 233;
of mud-furrows with shells, 237.
Catalogue of mineral springs, 315, 316.
Cataract of Niagara, 383.
Cattaraugus county, surface, rocks, etc., 488; timber, soil,
etc. 489.
Catskill group, 278.
Catskill shaly limestone, 144.
Cauda-galli grit, 150.
Caulophyllum, 451.
Cavities, 85, 87, 90, 98, 141, 142, 147, 150, 153,
Causes of the varying velocity in Niagara river, 386.
Cayuga lake, 406; marshes, 359, 416.
Cazenovia group, 184.
Cedars, 346.
Celestime, see Sulphate of strontian.
Ceratial rock, 162.
Ceraurus, 29.
Chalcedony, 67, 153, 157, 168, 456.
Chalybeate waters, 446.
Changes in the strata westward, 22, 514; of the Medina
sandstone, 39, 40.
Channels of streams, 297, 318.
Chara, 361, 468.
Characters of rocks between the Corniferous and Old Red,
176; of strata affecting the rate of recession in falls, 392.
Chasms produced by falls, 378.
Chautauque county, 220; surface, rocks, etc. 493.
Chautauque creek, 238.
Chautauque lake, 407, 493; former elevation of, 496.
Chawed rock, 162, 461, 466.
Chemung county, surface, rocks, etc. 477.
Chemung group, general character, 251; succession of strata
forming it, 253; section illustrating, 255; diagonal lamina.
tion and thickness of strata, 256; concretionary structure
of, 257; spheroidal desºluamation, 257; ripplemarks, 257;
localities, 258; thickness, 260; mineral contents, 260;
springs, 260; agricultural characters, 260; organic re-
mains, 261; localities of superposition, 276; local details
of, 467, 476, 477, 478,480, 485, 494; connexion with the
Old Red sandstone, 482; equivalency with the Waverley
sandstone of Ohio, 503; its varying characters, 253.
Chemung narrows, 478.
Chert, see Hornstone,
Chimney rock, 306.
Cincinnati, rocks at, 504, 505.
Clay, 227, 240, 418, 425, 437, 544, 467, 490; blue and yel-
low, 361 ; stratified, 344; green, 460.
Clay balls, 231.
Clay bank at Dunkirk, 362.
Clays, tendency to separate into laminae, 301.
Cleavages, 299.
Cliff limestone, 503, 506, 511, 512; equivalent of the Hel-
derberg rocks of New-York, 507.
Cliff in Portland, 328.
Clinton, De Witt, a patron and promoter of science, 7.
Clinton group, general character of, 58; subdivisions, 59,
60, 61, 62, 64, 65; localities, and thickness, 66; minerals,
67; mudcasts in, 67; organic remains, 68; localities of
superposition, 78, 79.
Clymenia, 293.
Coal, 239, 255, 452, 461; search for, 239, 452, 461, 467,
480; reasons of the fruitless search for, 8.
Coal conglomerate, attempted identification of the Oneida
conglomerate with, 6.
Coal formation, its non-existence in New-York, 4, 293; of
Illinois, or Wabash basin, 510.
Columnaria, 26.
Coldspring quarries, 448.
Compact calcareous blue shale, 184, 187.
Concentric iron seams, 288.
Concentric laminae separated and used for household uten-
sils, 257.
Concretions, 81, 85, 92–95, 128, 185, 192, 214, 219, 220,
227, 230, 231, 232, 239, 248, 257, 260, 287, 305, 458,
463, 473, 478, 480.
INDEX. * 667
Concretions or septaria, in Hamilton group, 193; in Gene-
see slate, 220; in Portage group, 230.
Concretionary structure, 214, 257; limestone, 480; sand-
stone, 227, 486. -
Conditions of deposition of the Hamilton, Portage and
Chemung groups, 254.
Conditions of the ocean and continents during the accumula-
tion of the older sedimentary deposits, 521.
Cone in cone, 232. -
Conesus lake, 198, 405, 407. -
Conglomerate, equivalent of the Millstone grit of England,
284; diagonal lamination, 286; concretions and seams of
iron ore, 287, 288; localities, 289; thickness, 291 ; or-
gamic remains, 291, 502; position regarding the coal
measures of Ohio, 292; associated with the Coal series,
292; local details of, 481, 486, 487, 488, 491, 494, 495,
- 501, 502.
Connexion of lithological character with features of surface
and soil, 14, 15. --
Conrad, Mr., his views of subdivision in the New-York
rocks, 24.
Continuation of species through successive formations, 10.
Contorted strata, 85, 86; seams of iron ore, 290.
Conularia, 110.
Copper pyrites, 44, 67; carbonate, 44, 67, 98.
Corals, 156, 460, 466,
Coral resembling Isis, 116.
Corniferous limestone, as a line of subdivision, 25; its
extent as a rock, etc. 161; ſaults in, 163, 450; character
of the strata, 166; localities, 167; thickness, 168; mineral
contents of, 168; springs in, 168; fissures in, 169; agri-
cultural characters of, 170; organic remains, 170; local
details, 450, 456, 460, 466, 471, 503.
Cornulites, 109, 137.
Corydalis, 451.
Cotting, Dr., survey of Georgia, 23.
Cranberry swamp, 416.
Crinoidal columns, 71, 77, 90, 151, 204.
Crinoidea, 65, 260, 466, 471, 486.
Crooked lake, 406. -
Crusoe island and lake, 416.
Cryphaeus, 200, 462.
Crystalline matter filling cracks in septaria, 193.
Cucullea, 196.
Current from north to south, 335; from south to north, 397.
Currents, evidences of, 320, 323, 397; polar, in ancient
ocean, 335.
Curved strata, see Concretions.
Curving joints, 305.
Cyathocrinites, lll, 247.
Cyathophyllum, 160, 462, 467.
Cyclas, 361, 396; 479. §
Cypricardia, 29, 30, 48, 76, 196, 256, 29ſ, 481.
Cyrtoceras, 29, 175. -
Cystiphyllum, 209.
Cytherina, 142, 421.
--~~ lº.
Dams, effects of artificial, 376.
Dark slaty fossiliferous shales, 184, 187.
Dark and green argillaceous shales, 230.
Darwin, Mr., his observations on climate, etc. in the southern
ocean, applied to explain the transportation of boulders,
335, --
Deep drift in Erie county, 469. x
Delthyris, 29, 70, 105, 137, 142, 148, 149, 171, 198, 200,
202, 205, 207, 208, 229, 245, 255, 256, 259, 269, 270,
276, 456, 467, 472, 481, 483,485, 486, 494.
Delthyris shaly limestone, 117, 144,
Deluge, universal, 339.
Dentaria, 451.
Detritus, superficial, 318; its origin, 321; its distribution,
319; local, 342.
Dewey, Prof. C., discovery of native copper in limestone of
Clinton group, 67. -
Devonian system, its equivalent in New-York, 20, 277.
Diagonal and curved lamination, 40, 41,230, 234, 256, 286,
290, 324. - --
Differences between strata of Europe and America of the
Same age, 8, 9. --
Different species inhabiting different parts of the ocean, 186.
Diluvium, 318. -
Dip of rocks of the Portage group, 239; of rocks along the
Niagara river, 387; of strata, 296.
Dipleura, 205.
Direction of grooves, 327; of ripplemarkings, 49.
Disappearance of streams, 169. •
Discoloration of sands and clays from percolating water,
163, 361.
Distinctions between the Hamilton and Chemung groups,
276.
Distribution of boulders, 332.
Dogtooth spar, 86, 92, 98, 168.
Drab limestone, 119.
Drainage of Lake Erie, 400.
Drift, 46, 126, 179, 318, 482.
Drift hills of Monroe county, 423.
Drift deposit at Lewiston, 441.
Drift and boulder formations, their relative age, 338.
Ducatel, Prof. & J. H. Alexander, geological and topogra-
phical survey of Maryland, 23. --
Dudley limestone, its equivalent, 81.
Dunkirk harbor, 329.
IE,
Eaton, Prof. A., his survey of the New-York rocks, 5; his.
opinion of the age of the same rocks, 5, 6; his index to the
geology of the Northern States, 6; agricultural survey of
Albany and Rensselaer counties, 6; section of the rocks
from Lewiston to Lake Erie, 395. --
Effect of woodlands on springs, 239; of winds on lake levels,
410.
Efflorescences, 98, 312.
668
INDEX,
Elevated country in Canada, 337.
Elevated lakes, 252.
Elevation of the hills of the Chemung group, 252; of the
tertiary on Lake Champlain, 337; of the Ridge road above
Lake Ontario, 351; of rocky strata by the freezing of
water, 375; of the ancient ocean, 353; and depression of
the waters of the Great lakes, 408.
Elevation of Monroe county, 422; of Orleans county, 434;
of Allegany county, 484; of Chautauque county, 493.
Elevation and submergence, evidences of alternate, 321.
Ellipsolites, 28,
Encrinal limestone, 145; of the Niagara group, 89; of the
Hamilton group, 184, 187, 189, 204, 492.
Epsomites or lignilites, 130.
Erie county, rocks of, etc. 469.
Erie lake, future drainage of, 400.
Erratic blocks, 424.
Erroneous opinions regarding the nature of the earliest fos-
sils, 10.
Errors in identification of strata, 7.
Euomphalus, 28, 109, 137, 172, 291.
Evidences of a current from south to north, 397; of the
former existence of deep lakes in certain river valleys,
343; of higher elevation in many water courses, 353; of
ancient currents, 457.
Extent of the Old Red sandstone, 179.
Extinction of species, 9, 367.
I F.
Facilities for communication in Steuben county, 48l.
Falls, 225, 377; Genesee lower, 382; Hector, 379; Nia-
gara, 383; Portage, 224, 368; Portage lower, 370; Ro-
chester upper, 82, 85; Shelby, 83, 88; Taghannuc, 377.
Falls, recession of, 378, 381; past recession of the Niagara,
390; future recession of the same, 398.
Fauna of the deep and distant parts of the ocean more likely
to be uniform and unchanged than near the shore, where
subjected to the invasion of variable deposits, 515,
Favosites, 29, 157, 159, 462, 467.
Ferns in the Chemung group, 476.
Ferriferous slate and limerock, 58.
Fields covered with boulders, 332.
Filicites, 273.
Fine beach sand covering conglomerate, 495.
Firestones, 62, 65, 147, 420, 432, 456, 467, 483.
Fishes, remains of, 278, 487; fossil, found in the central
portion of the Transition or Silurian strata, 10.
Fissures in the Corniferous limestone, 169.
Flagstones and shale of Gardeau, 227.
Flagging stones, see Building and flagging stones.
Flagging stones, 448, 452, 458, 476, 477.
Flat gravel, 240, 260, 323, 324, 474, 488.
Fluid bitumen in concretions of Marcellus shale, 221.
Fluor spar, 28.
Fluviatile deposits of Goat island and the hanks of Niagara
river, 396, 397.
Fossil bones of quadrupeds, 363, 364.
Fossil characters of strata, value of, 501,
Fossiliferous iron ore, 60.
Fossils not found in the gypseous rocks, 460; rarely accom-
pany rippled surfaces, 477; of the older rocks, allied to or
identical with Trochus, Turbo, Nucula, Avicula, &c. 10.
Fossils of the Potsdam sandstone, 27; of the Calciferous
sandrock, 28; Trenton limestone, 29; Utica slate, 29;
Hudson-river group, 30; Medina sandstone, 46; Clinton
group, 68 - 77; Niagara group, 100 – 117; Onondaga-salt
group, 137, 138; Water-lime group, 142; Oriskany sand-
stone, 148, 149; Onondaga limestone, 157 – 160; Cormi-
ferous limestone, 170 – 175; Marcellus shale, 180 – 182;
Hamilton group, 195 – 210; Tully limestone, 215, 216,
Genesee slate, 221 – 223; Portage group, 241 - 247;
Chemung group, 261-275; Old Redsandstone, 280–283;
Conglomerate, 291, 292.
Fossils common to the Clinton and Niagara groups, 75.
Fossils, changes in corresponding to lithological changes,513.
Fossils, diminution of in the higher groups in a westerly
direction, 514.
Foster, J. H., report on the geological survey of Ohio, 25.
Fourth geological district, limits of, l; rocks not reaching to
any previously well known limit downward, 26; physical
features of, 405; sources of prosperity in, 499.
Fredonia, 228 ; lighted by gas, 498.
Freezing water, action in deepening river channels, 375.
Fucoides, 28, 46, 69, 77, 228, 229, 241, 247, 439, 480.
Furrows and striae in conglomerate, 286.
Furrows, oblique, 331. ?
Future subdivisions to be made in groups, 3.
Głs
Galena (see Sulphuret of lead), 431.
Gardeau shale and flagstones, 224, 227, 463, 467.
Gardeau slide, 463.
Garnet sand, 426.
General features of the strata and physical characters of the
Fourth district, 12, 13.
Genesee county, rocks of, etc. 464.
Genesee falls, recession of, 381.
Genesee flats, 334.
- Genesee river, 124.
Genesee slate, 188, 226; general characters, 218; extent,
etc. 219; concretions of, 220; localities, 220; thickness,
221; minerals of, 221; organic remains, 22ſ; local details
of, 452, 457, 458, 462, 467, 473.
Genesee valley, 189, 217, 220, 372.
Geodes, see Cavities.
Geodiferous limerock, 80.
Geology of New-York, knowledge of, previous to the com-
mencement of the present survey, 7.
*
INDEX.
669
Geological labors in America to identify rocks with those of
Europe, 5.
Geological formations of Europe and America, cause of dif-
ficulty in attempting to harmonize the arrangement in the
two countries, 8.
Geological position of the lead ores of Wisconsin, Illinois
and Iowa, 512. &
Geological examinations in Maine and Massachusetts, 22;
in Connecticut, New-Jersey, Pennsylvania, Virginia,
Maryland, Delaware, Ohio, Michigan, Indiana, Illinois,
Wisconsin, Iowa, Tennessee, Georgia, North and South
Carolina, 23.
Geological position of the western lakes of New-York, 406;
of Lake Ontario and Lake Erie, 408.
Glaciers, 330, 334.
Goat island, 97, 347, 395, 396.
Goniatites, 229, 243, 245.
Gorge of the Niagara river, 388; from the Whirlpool to St.
David's, 389; of Bloody run, 396, 398; of Wölf creek,
374; of Canaserowlie creek, 380.
Gorgomia, 115.
Grand island, 127.
Graptolites, 29, 30, 72.
Gravel (see Drift), 319, 474.
Grazing lands, 240, 261, 294. **
Great lakes, relative elevation of, 384; elevation and de-
pression of water in, 408.
Green bands and spots in Medina sandstone, 38, 117, 120.
Green marl, 189, 120. ?
Green varieties of shale increasing west of Genesee river,
253, *-*.
Green varieties of shale not slaty, 230.
Greenish grey argillaceous or siliceous sandstone, 39.
Greentown in Ohio, coal beds and associated limestone, 502.
Grey quartzose sandstone, 37. $4
Grey sandstone and Oneida conglomerate, 31.
Grey sparry limerock, 151.
Greywacke, 117, 177, 184.
Grindstones, 483, 585, 495, 497.
Grif, Schoharie, 151; Cauda-galli, 150.
Grit slate of Eaton, 151.
Grooved, striated and polished rocks, 325; on Lake Erie
shore, 328; surface of limestone in Clintom group, 329.
Groove 100 feet long at Lockport, 327.
Grooves, direction of, 325, 327; remarks on the theories
regarding, 330.
Groups of the Fourth district, 32; below the same, 26.
Gypseous marls and slates, -- 117, 120, 418, 426, 449, 453,
464; rocks used as marl, 429.
Gypsum, 98, 120, 121, 122, 123, 124, 125, 421, 430, 449,
450, 453, 454, 455, 457, 460, 465, 469, 480.
FI,
Hamilton group, general characters, 185; subdivisions, 187;
extent, 188, 189; jointed structure or vertical cleavage,
192; concretions or septaria, 193; localities, 193; thick-
mess, 194; mineral contents and springs, 194; agricultural
|GEoL. 4th DIST.]
---
85
characters, 194; organic remains, 195; localities of super-
position, 211 ; local details of, 451,457, 458,462, 467, 503.
Hardpan reclaimed by manuring, 468. -
Hayes, Mr., his speculations regarding Niagara falls, 395.
Hearthstones, 483.
Hector falls, 379, 476.
Helderberg group, 144.
Helix, 437, 479.
Hemicrypturus, 77.
Hemlock lake, 407.
Hennepin, Father Louis, account of Niagara falls, 394.
Hildreth, Dr., papers on the geology of Ohio, 23.
Hipparionyx, 149, • *-
Hitchcock, Prof., survey of Massachusetts, 22,
Holoptychus, 281, 282, 482.
Homalonotus, 103.
Homeoye lake, 407. ---
Hopper hills, 194.
Hopper-shaped crystals and cavities, 127, 128.
Horizontal position of strata considered an indication of
more recent age of rocks, 9.
Hornstone, 63, 67, 87, 162, 165, 168, 471.
Houghton, Dr. D., geological survey of Michigan, 23.
Howard flats, 482. .*
Hudson river group, 30; identity of the Blue limestone of
Ohio with, 503, 504. arº
Hydraulic cement, 142, 431, 447, 455, 480.
Hydraulic lime, 84, 85, 88, 128 – 130, 182, 143, 147, 424,
438, 455, 465, 470, 471. ^---
Hydraulic limestone, transported blocks of, 341.
Hydrosulphuretted springs, 427.
Hypanthocrinites, 113. -
Hypogene or Primary system, 17.
M.
Icebergs and floes, see Glaciers.
Ichthyodorulite, 174, 175, 456,
Identity of the rock formations of New-York with those of
the Western States, 500; with those of Europe, 516/
Identity of strata in Russia, Siberia, Sweden, Norway,
Canada, &c. 21. *.
Illaemus, 29.
Inachus, 29.
Increase of calcareous and diminution of sedimentary matter
in a westerly direction, 515.
Index to the geology of the Northern States (Eaton's), 6.
Iodine in brime springs, 315.
Iron ore, 486; bog and argillaceous, 140, 419, 437, 447, 470,
491; boulders of, 491; concentric seams of, 288; fossili-
ferous, 60.
Iron, native, 459; sulphate, 260, 312 ; sulphuret, 44, 64, 67,
81, 98, 99, 157, 179, 239, 296,297, 479, 480, 483; oxide,
64; hydrated peroxide, 44, 287.
Iron pyrites, see Sulphuret of iron.
Iron pyrites replacing fossils, 182, 189, 192, 193, 260.
Iron pyrites mistaken for silver, 669,
Iron sand, 476.
f
670 INDEX,
Irondequoit and Genesee, relative elevation of 422.
Ischua stone quarries, 492.
Isotelus, 29.
Ithaca group, 250.
Jºe
Jackson, Dr. C. T., surveys in Maine, Rhode-Island and
New-Hampshire, 22. a-
Java lake, 407.
Joints, 163, 168, 192, 237, 239; their effect on vegetation,
169; in the vicinity of uplifts, 300; cause of, 301; inter-
rupted by interstratified sandstones, 304; dividing fossils,
302; useful in quarrying, 302; vertical and striated, 331.
Jointed structure of the rocks in the Fourth district, 299;
of the limestones, 302; of the shales and sandstones, 303;
of the conglomerate, 307.
HK,
Knowledge of the rocks of New-York at the commencement
of the survey, 7.
ILe
Lakes, 405; tables of elevation, length, breadth, etc. of, 411,
412,413 ; in Chautauque county, former elevation of, 496;
elevation and depression of water in the Great lakes, 408;
their relative elevation, 384; extent of the valley of St.
Lawrence, 407.
Lake, Bear, 407; Canadice, 407; Canandaigua, 121, 189,
407; Cassadaga, 407; Cayuga, 121, 188, 212, 406;
Chautauque, 407; Conesus, 405, 407; Crooked (Kewka),
188,213, 220, 406; Hemlock, 407; Honeoye, 407; Java,
407; Loon, 482; Seneca, 188, 212, 221, 227, 406; Silver,
407.
Lake Erie, future drainage of, 400.
Lake levels, annual fluctuation of, 410; effect of winds on,
410.
Lake marl and tufa, 360.
Lake ridges and beaches, 348; modern, 354 – 356.
Lake shore in Monroe county, 423; in Niagara county, 442;
and streams in Orleans county, 434; above Buffalo, 472.
Lateral movements of strata, evidences of 296.
Elead, sulphuret, 86, 134, 194, 221.
Lead ores of Wisconsin, Illinois and Iowa, 512.
Lenticular clay iron ore, 60.
Lewiston terrace, grooved rocks of, 329.
Lighthouse at Portland harbor, 498.
Lignilites, 95, 130; see Epsomites.
Lima, 264.
Lime, 466, 472, 484; sulphate (see Gypsum), 99, 120–128,
134, 311, 477; carbonate in crystals, 65, 67, 84, 96, 131,
214, 239.
timestone, Birdseye, 28; Black-river, 28; Carboniferous,
19, 179, 411, 508, 511; Chazy, 28; Corniferous, 161,450,
508; Delthyris shaly, 144; Encrinal, 145; Niagara, 84;
Onondaga, 151; Pentamerus, 144; Trenton, 29; Tully,
212; Upper Pentamerus, 145.
Limestone, of Clinton group, 62, 65; argillaceous and em-
crimital, 481 ; concretionary, 480; oolitic, 508; vermicular
or porous, 128; carboniferous, its absence in the Eastern
States, 8; of Black-Rock and Niagara, considered as the
same, 8; Blue of Ohio, its identity with the Hudson-river
group, 503, 504; Cliff, 503, 506, 511 512.
Lines of deposition, 230.
Lingula, 28, 29, 48, 52, 76, 77, 108, 222; one of the earliest
known fossils, and existing in our present seas, 10.
Lithological changes accompanied by fossil changes, 33.
Lithological characters of strata, value of, 501.
Little ridge, 350.
Littorina, 72, 142,
Livingston county, rocks of, etc. 459.
Llandeilo flags, equivalent to the Utica slate, 29.
Local geology, 414, 422, 433, 440, 449, 453, 458, 459, 464,
469, 475, 477, 480, 484, 488, 493.
Localities of the Chemung group, 258, 276; of the Clinton
group, 66 ; Genesee slate, 220; Hamilton group, 193,211;
Marcellus shale, 179, 183; Medina sandstone, 42; Nia-
gara group, 96; Old Red sandstone, 280; Onondaga
limestone, 156; Onondaga-salt group, 118; Portage group,
237, 248; Tully limestone, 214.
Locke, Dr., report on the geology of Ohio, 23.
Lockport, 83, 88, 99, 100.
Lockport limestone, 80.
Long pond, 356.
Lower falls of the Genesee, 382.
Lower green shale, 59, 60.
Lowest position of remains of fishes, 145.
Loxonema, 137, 200, 256.
Lucina, 245.
Ludlow formation, equivalent to the Chemung group, 278.
Ludlowville shales of Hamilton group, 187.
Lymnea, 361, 396, 479.
Mºe
Mackinaw, 118 ; rocks at, 512.
Maclure, Mr., his labors on the geology of the U. States, 4.
Maclurea, 28.
Madison, Indiana, rocks at, 506.
Magnesia, 63, 96, 98, 130.
Magnesian deposit, 117, 128, 141.
Magnesian character of the Niagara limestone, 84, 85.
Magnetic iron sand, 426.
Manchester sulphur springs, 313.
Mangamese, oxide, 44, 260, 490.
Manures, their application, 240.
Maple ridge, 434.
1Marble's quarry, waterworn rock at, 415.
Marble, variegated of Lockport, 448.
Marcellus shale, general characters and subdivisions, 177;
localities and thickness of, 179; minerals and springs,
179; agricultural characters, 179; organic remains, 180 ;
localities of superposition, 183; loeal details of, 451, 457,
461, 466, 472, 503, 508.
Marl, -- 360, 487, 446, 453, 457, 464, 468, 477, 479, 484,
490, 496; gypseous, 418; its origin, 360; great deposit in
Livingston county, 463; and tufa, 360, 428, 491.
Marshes, elevation of, 357; and swamps, 416; Cayuga, 359,
416.
INDEX, 671
Marsupiocrinites, 113.
Mastodon, bones and teeth of, 363 — 365; recent existence
of, 365; position of its bones, 367.
Materials for construction, 432, 447; see Building stones.
Mather, Prof. W. W., geological survey of Ohio, 23.
Maysville, Kentucky, rocks at, 503.
Means of transport, conditions of the surface, etc. 334,
Medina sandstone, general characters of, 34; extent in the
Fourth district, 35; subdivisions of, 36–39; diagonal and
curved lamination of, 40, 41; accretions in, 41; localities,
42; thickness, 43; minerals and springs of, 44; saline
springs, 44; agricultural characters of, 45; organic remains,
46; ripplemarks, 49 ; shrinkage cracks, 51; evidence of a
beach with stranded shells, 52; wave-lines, 54.
Medina sandstone mistaken for red shale of the Salt group,
35; blocks of, on Niagara limestone, 340.
Melania, 396.
Metals, 430, 447. •x
Mica, 483.
Micaceous sandstone, 492.
Michigan, rocks of, 512.
* Microdon, 196.
Minerals of the Chemung group, 260; of the Clinton group,
67; Corniferous limestone, 168; Genesee slate, 221 ;
Hamilton group, 194; Marcellus shale, 179; Medina
sandstone, 44; Niagara group, 98; Onondaga limestāne,
157; Onondaga-salt group, 124; Portage group, 239;
Tully limestone, 234. $
Mineral and gas springs, 308; catalogue of, 315, 316.
Mineral waters, 417.
Mitchill, Dr., obtained the first collection of minerals from
New-York, 7.
Mitella, 451.
Modern superficial detritus, 342.
Modern action of rivers, 369,
Modiola, 196.
Monroe county, rocks of, surface, etc. 422.
Montrose sandstone, 278.
Moraines, 357.
Moscow shale, 187, 472.
Mountain crystallization, 30l. ~
Mountain ridge, 348.
Muck, 359, 423, 468, 484; swamps, 359,
Mudcasts in Clinton group. 67.
Mud-furrows, 237, 476.
Mudstone, 189.
Murchison, Mr., results of his labors, 20, 21.
Murchison and Verneuil, investigations in Russia, 21.
Muriate of soda, see Soda. *
No.
*
Names, local, 23.
Negative knowledge useful, 4.
New channels formed by rivers, 377.
New-York rocks, extent, etc., overlaid by no formation more
modern than the coal, 24; their diminution to the westward,
22.
New-York system, subdivisions of 18; equivalent to the
Transition of Werner, 20,
New Red sandstone and Tertiary, 317.
Niagara county, rocks of, surface, etc. 440.
Niagara falls, 80, 96; its past, present and prospective con-
dition, 383; recession of, 390, 398; table of observations
on the present position of, 404; section of 397; trigono-
metrical survey of, 402; monuments erected near, 402.
Niagara group, general features of, 80; subdivisions of, 81,
84; topographical features of, 96; localities, 96; thickness,
97; minerals of, 98; springs in, 99; agricultural charac-
ters, 99; organic remains, 100.
Niagara limestone, its mode of formation, 87; striated sur-
face of 95; thickening of strata, 92; concretionary struc-
ture of, 86, 93, 94; geodes in, 86; encrimal columns in,
90; subdivisions near Rochester, 87; subdivisions at
Lockport, 89; Porites with linear cavities, 90.
Niagara river, 83, 97; quantity of water flowing in, 401 ;
water abstracted by the canals, 40k.
Niagara sandstone, 34.
Nicollet, Mr., his investigations west of the Mississippi, 23.
Nitrogen gas, 308, 451.
Nomenclature, objects of, 2.
Non-existence of the Coal formation in New-York, 4.
Nucula, 29, 30, 76, 196, 245.
Nunda, 217.
Nunda group, see Portage group.
Gºs
Oak openings, 137.
Oak-orchard creek, 393.
Objects of the survey, 2,
Odontocephalus, 175.
Oil spring, 491.
Old Red sandstone, or Old Red system, 19; recognized by
Mr. Eaton, 6.
Old Red sandstone, general characters, 278; position with
regard to the Côal measures of Pennsylvania and Indiana,
278, 280; localities of, 280; organic remains, 290; con-
nexion with the Chemung group, 482; an impure iron ore,
482.
Olive or bluish fissile shale of the Hamilton group, 117.
Olmstead, Prof., survey of North-Carolina, 23.
Oneida conglomerate and Grey sandstone, 31.
Oneonta sandstone, 278.
©nondaga limestone, extent and general characters, 154,
152; localities of, 156; thickness and minerals of, 157;
organic remains, 157; local details of, 456, 460, 466,474.
Onondaga-salt group, general characters of, 117; localities,
I18; subdivisions, 119, 120; plaster beds, 121 – 125;
porous limestone, 128; upper deposit, 128; ligmilites or
epsomites, 131 ; shrinkage cracks, 133; minerals, 134;
brine springs, 134; wells and springs, 136; agricultural
characters, 136; organic remains, 137; localities of super-
position, 139, 140; local details of, 422, 449, 453, 459,
464, 469.
Ontario county, rocks of, etc. 453,
672 INDEX,
Oolitic limestone and sandstone, 508.
Oolitic or argillaceous iron ore, 60, 61, 69.
Ophileta, 28. ---
Orbicula, 28, 48, 108, 180, 222, 256, 461; one of the earliest
fossils, and an existing genus, 10.
Ore used for paint, 419.
Organic forms, their rarity in the western waters from the
termination of the Corniferous limestone to the commence-
ment of the Carboniferous period, 514.
Organic remains of the Chemung group, 261; of the Clinton
group, 68; Corniferous limestone, 170; Genesee slate,
221; Hamilton group, 195; Marcellus shale, 183; Medina
sandstone, 46; Niagara group, 100; Onondaga limestone,
157; Onondaga-salt group, 137; Oriskany sandstone, 148,
149; Old Red sandstone, 280; Portage group, 241; Tully
limestone, 215; Water-lime group, 142; not found in the
clays of Lake Ontario, 317.
Organic remains of the Blue limestone of Ohio, identical
with those of the Hudson-river group of New-York, 504.
Oriskany sandstone, general characters, 146; absence in the
Fourth district, 146; thickness in Pennsylvania, 147;
organic remains of, 148, 149; locality in Ontario county,
456.
Orleans county, rocks of, surface, etc. 433.
Orthis, 28, 29, 30, 71, 105, 142, 175, 180, 215, 229, 245, 255,
256, 267, 461, 494.
Orthoceras, 28, 29, 30, 110, 137, 180, 243, 418, 461.
Orthomota, 76, 205.
Orthonychia, 172.
Oswego river, the common outlet of four lakes of the Fourth
district, 406.
Owen, Dr. D. D., report on the geology of Indiana, 23.
*-
EP,
Paint ore, 419.
Paracyclas, 171.
Parallel ridges, 357.
Pearl spar, 92, 98.
Peat, 442, 490.
Pecten, 264.
Pénnsylvania survey, No. 1, 27; No. 5, 34; No. 6, 80, 144,
T45; No. 7, 146; No. 8, 177, 184, 218; No. 9, 224, 251;
No. 11, 278.
Pentamerus, 70, 382, 422.
Pentamerus limestone, 62, 144.
Percival, Dr. & Prof. C.U. Shepard, survey of Connecticut,
23.
Petroleum, 168, 497, 498.
Philipsburgh, rocks at, 486.
Pholas costata, a bed of the shells found at New-Bedford,
but the species not now known in a living state, 9.
Physical advantages of New-York, 410.
Physical features of the Fourth district, 405.
Pinnopsis, 243.
Planorbis, 361, 396, 479.
Plaster or gypsum beds, 121 – 125.
Plaster, its action on vegetation, 430.
Pleurorhyncus, 171.
Pleurotomaria, 28, 29, 48.
Ponds, 169, 170.
Porites, 86, 91.
Portage falls, 368; lower falls, groundplan of, 37.
Portage or Nunda group, general characters of, 224; sub-
divisions, 226; diagonal lamination, 230; ripplemarks,
230; casts of shrinkage cracks, 230; concretions, 230;
casts of flowing mud, 232; casts of mud-furrows and
striae, 234 ; localities, 234; thickness, 238; minerals and
springs of, 239; agricultural characters, 239; organic
remains, 241; localities of superposition, 248; summit of,
260; local details of, 452, 457, 458, 467, 473, 477, 480,
484, 488, 494.
Portage group equivalent of Waverley sandstone, 50l.
Posidonia, 72.
Potholes, 376.
Potsdam sandstone, 27.
Prairies, 321.
Primary or Hypogene system, 17.
Protean group, 58, 80.
Protozoic rocks, the first great division, 24.
Pseudomorphous or hopper-form crystals and cavities, 127.
Pterinea, 29, 30, 172, 229, 254.
Pyrites, 477; see Iron pyrites.
Pyritiferous rock, 177, 184.
Quantity of water flowing down the Niagara river, 401.
Quarries, 38, 451, 460, 478, 488, 492, 497.
Quartz crystals in Calciferous sandrock, 28; in Clinton
group, 67; in Onondaga limestone, 153, 157, 168.
Quaternary system, 19.
Queenston heights, 384. r
Quicklime, 84, 85, 88, 420, 438, 467; and hydraulic cement,
431.
Quicksand, 346.
Hêe
Rapids between Lake Erie and Niagara falls, 400.
Ravines of Chautauque county, 253; in the Hamilton group,
451; at the head of Canandaigua lake, 457.
Recession of falls, 378; of Niagara falls, 391, 398.
Red and variegated shales and sandstones of Pennsylvania,
58. ,
Red marl and sandstone, 34. w
Red marly and shaly sandstone, 36. $.
Red sandstone of Oswego, 34. ~
Red shale of the Onondaga-salt group, 119.
Red shale and sandstone, 38. -
Relative elevation of Northern and Western New-York, 335.
Relative ages of modern deposits, 342.
Remarks preliminary to the rocks above the Tully limestone,
217. -- —º
Rensselaer School, establishment and objects of, 6.
Resources of the northern counties, 498; of the southern,
498.
Rhomb spar, 134.
INDEX,
673
Ridges, parallel, 357; morth and south, 341; not found north
of the Ridge road; and beaches, modern, 354.
Ridges (lake), in Ohio and Michigan, and their elevation,
351; remains of wood in the sand of, 349.
Ridge roads of Lakes Erie and Ontario, 348, 349, 414 ;
division of the ridge in Niagara county, 350.
Ripplemarks, 49, 230, 257, 476. -
Rippled surfaces in Steuben county, 480.
River courses changed by superficial materials, 389.
Rivers, new channels formed by, 373.
Rochester, 98, 99, 100.
Rochester shale, 80.
Rock city, 285, 289.
Rock formations of the Western States, identity with those
of New-York, 500.
Rocking stones, 341.
Rogers, Prof. H. D., surveys of New-Jersey and Pennsyl-
vania, 23; paper on the Falls of Niagara, 395.
Rogers, Prof. W. B., survey of Virginia, 23.
Roy, Mr., his examination of ancient beaches, 353.
Rutile, 99.
z
&
§.
Saliferous group of Onondaga, 453.
Saliferous rock, 34.
Salines, or brine springs, 314; their origin, 127; of the
Medina sandstone, 44.
Salmon river, 317.
Salt springs, 45, 418, 427, 436, 446, 484, 491; of Salina,
their geological situation confounded with those bordering
Lake Ontario, 8,
Salt springs supposed to increase instrength on descending,
446.
Sand, 426, 445, 487; between layers of rock, 329; used in
hydraulic cement, 143; and gravel, see Drift.
Sandbars, removal of, 409.
Sandrock, calciferous, 28. -
Sandstone, Potsdam, 27; Grey, 31; Medina, 34; Oriskany,
146; Old Red, 278; New Red, 317; Portage, 225, 226,
228; Niagara, 34; Oneonta, 278.
Sandstone, concretionary, 485, 492; red, marly and shaly,
31 ; grey, quartzose, 37; red shale and, 38; greenish,
grey, argullaceous, 39; bituminous, 310, 485; with oolitic
limestone, 508; olive shaly, 248; micaceous, 492.
Sandy beach and stranded shells, 52, 53, 290.
Sanguinolalia, 317.
Sauripteris, 281, 282.
Scenery of the Medina sandstone, 35.
Schohalie grit, 151.
Scutella limestone, 145.
Second great division of the New-York rocks, 24.
Second green shale, 64.
Sedimentary deposits, their influence on organic forms, 249.
Selenite, 90, 98, 120, 453, 480,
Selenurus rock, 170.
Seneca county, rocks of, etc. 449.
Seneca lake, 406. |
[GeoL. 4th DIST.] 86
Seneca limestone, 161.
Seneca oil, see Petroleum.
Seneca river, ancient course of, 415.
Septaria, see Concretions.
Shale, Rochester, 80; Marcellus, 177; Ludlowville, 184,
187; Skaneateles, 184; Sherburne, 184, 224; Cashaqua,
218, 224, 226, 462, 467, 473; Hamilton, 225; Moscow,
187, 472; Chemung, 252; Niagara, 81; second green of
Clinton group, 64; lower green of ditto, 59.
Shale, dark slaty fossiliferous, 187; carbonaceous, 84;
compact calcareous blue, 187; olive or bluish fissile, 187;
red, and sandstone, 38; black bituminous of Ohio and
Indiana, 508 ; and flagstones of Gardeau, 227; black
micaceous, 248, 485.
Shales become thin west of the Genesee river, 190; extend
from the east to Lake Erie, 191; used as plaster, 463.
Shells stranded on a sandy beach, 52; freshwater, at the
Whirlpool, 403.
Shell grit, 148. -
Shell limerock, 107.
Shell marl, 428, 479.
Shepard, Prof. C.U. & Dr. Percival, survey of Connecticut,
23.
Shot ore, 438.
Shrinkage cracks, 51, 133, 147, 230.
Sigillaria, 275.
Siliceous sinter, 67. .*.*.
Silicified shells, 63.
Silurian system, equivalent to the Hamilton group, 20.
Silver lake, 407.
Slate, Genesee, 218; Utica, 29; Calciferous, 80, 117.
Slide, Gardeau, 463.
Slippery-rock creek, 409.
Smooth surfaces of grey quartzose sandstone, 37.
Soda, muriate, 98. –
Sodus point iron ore, 62.
Soil, 99, 105, 179, 240, 416, 424, 435, 443, 453, 473, 474,
481, 843, 490, 495, 496.
Sources of prosperity in the Fourth district, 499.
Spar, see Carbonate of lime. *r
Sparganium, 357.
Spermaceti-like substance in concretions of Genesee slate,
227.
Sphenopteris, 275.
Spheroidal desquamation, 257.
Springs, 99, 136, 426, 436, 445.
Springs, Caledonia, 170; Canoga, 170, 308.
Springs in the Medina sandstone, 44; in the Niagara group,
99; and wells of the Onondaga-salt group, 136; in the
Corniferous limestone, 168; of the Marcellus shale, 179;
in the Hamilton group, 194; Portage group,239; Chemung
group, 260.
Springs, salt, 417,427, 436, 446, 484, 491 ; mineral and gas,
308; evolving carburetted hydrogen and petroleum (burning
springs), 309, 310; nitrogen, 308; sulphuretted hydrogen,
311 ; brine or saline, 314; sulphur, 417, 436, 445, 491; in
674
INDEXe
Virginia, 309; and mineral waters in Orleans county, 436.
Springs, catalogue of mineral,315; influence of woods upon,
260; temperature of, 308, 313; rising along limes of frac-
ture, 309; water and, 445. -
Steuben county, rocks of, surface, etc. 480; facilities of
communication, 481.
Stokes on the Orthocerata, 21.
St. Lawrence river, 335. -
St. Louis, limestone at, 500.
Stratified clay, 344. .
Streams, wearing power of, 371; outlets closed during
storms, 355, 358.
Striated, grooved and polished rocks, 325.
Striated surfaces, 318, 322, 824–7, 331.
Strombodes, 209.
Strontian, sulphate, 86, 98, 131, 134, 460.
Strophomena, 28, 29, 30, 72, 77, 104, 171, 175, 180, 200,
222, 255, 266, 276, 461, 467, 472, 481, 483, 486.
Succession of rocks along Niagara river, 387.
Sulphate of lime, 477.
Sulphur, native, 99, 312.
Sulphur springs, 417, 470, 491; of Avon, 313.
Sulphuretted hydrogen, 99, 427; springs, 341.
Sulphuric acid springs, 134, 136.
Superficial detritus, 318; origin and mode of formation, 318;
of older rocks diminishes to the southward, 319; princi-
pally composed of the strata occupying the district, 320;
sections illustrating the character and position of 322,
323; evidence of several periods of deposition, 324;
modern, 342; section showing the position of, 345.
Surface markings of Medina sandstone, 50.
Survey of Canal rocks (Eaton's) quoted, 5.
Sutures, 131.
synclinal axis of the Wabash valley, 513.
Syringopora, 160.
T.
Table of observations showing the present position of Niagara
falls, 404.
Tables of elevation, areas, etc. of the lakes of New-York,
411 – 413. -
Tabular arrangement of the rocks of the New-York system,
17.
Table rock, 399,
Tacomic system, 17.
Tellina, 196.
Tentaculites, 72, 142, 172, 180, 222, 256.
Tentaculite limestone, 141.
Termination of the great limestone formations of New-York,
175; of the shales of the Hamilton group, 188, 212.
Terrace produced by subsiding water,352; along Lake Erie,
351; at Lewiston, 441; near Black-Rock, 397; in the
valley of Chautauque lake, 496.
Terraces, 88; with freshwater shells, 396; formed by de-
nudation, 385.
Terraced hills, 352.
Terreme vegetation, no evidence of it in the lower rocks, 254.
Tertiary, 19; and New Red sandstone, 317.
Testacea in marl beds, 361.
Third great division of New-York rocks, 25.
Tiarella, 451. f
Tide waters at Albany, 410.
Timber, 100, 137, 240, 344, 346, 416, 461, 474, 489, 492.
Tioga, Pennsylvania, rocks at, 482.
Tompkins county, rocks of, etc. 475.
Topographical features of the Fourth district, 13; change
in, due to change in the nature of the strata, 14.
Topography of Monroe county, 422; of Orleans county,433;
Niagara county, 440; Erie county, 470; Chemung county,
479; Steuben county, 480; Chautauque county, 493.
Trap dykes, 295.
Transition of Werner, 20.
Trenton limestone, 29. -
Trigonometrical survey of Niagara falls, 402.
Trillium, 451.
Trilobites the first created animals possessing highly de-
veloped locomotive powers, 10,418.
Troost, Dr. G., survey of Tennessee, 23.
Tufa, 99, 359, 360, 427, 428, 446, 453, 468, 484, 490, 491.
Tully limestone, general characters, 212 ; concretionary
structure, 214; localities and thickness of, 214; mineral
contents, 214; organic remains, 215; local details, 452,
457, 458, 473, 476.
Turbo, 198.
Ue
Undulations, 92, 123, 213, 298.
Ungulina, 243.
Unio, 396.
Uplifts, 295 – 297, 328.
Upper limestone of Clinton group, 65.
Upper Pentamerus limestone, 195.
|Utica slate, 504; and associated beds of limestone, 29.
We
Walleys, 15, 187, 225, 252, 459, 489; of drainage and ero-
sion, 405. -
Walleys of Ontario, St. Lawrence and Champlain, 317; of
Seneca, Cayuga, Crooked and Canandaigua lakes, 321;
in Cattaraugus county, 489; in Chautauque county, 496.
Valley of the Genesee river, 344.
*
.Valvata, 361, 396.
Van Campen's creek, sandstone on, 486.
Wandemark’s creek, rocks of, 486.
Van Rensselaer, Stephen, his patronage of science, 5.
Wanuxem, Prof. L., geological survey of South-Carolina, 23;
on the identity of western rocks with those of New-York,
500.
Variegated marble of Lockport, 448.
Variegated sandstone, 34.
Vegetable remains, 239, 275, 452, 480.
Werneuil and Murchison, investigations in Russia, 21.
Wertical cleavage, see Joints.
INDEX. 675
W.
Wad, or earthy oxide of manganese, 260, 491.
Water, freezing, its action in deepening new channels, 375;
acid, 464.
Water, quántity flowing in the Niagara river, 400; quantity
taken therefrom for the canals, 401; transporting power
of, 335; larger area accompanied with more uniform
temperature, 335; and springs, 126, 445; mineral, 436.
Water-courses, direction of, 15.
Waterfalls, 377.
Water lime, or hydraulic cement, 142.
Water-lime group, general characters of, 141; linear cavities
from the solution of crystals, 142; organic remains, 142.
Wave-lines in Medina sandstone, 54, 55; on recent beaches,
56. z
Waverley sandstone of Ohio, 229; equivalent to the Portage
group, 50l.
Wayne county, rocks of, etc. 414, 415.
Wearing action of falls and streams, 371, 394.
Wedge-form layers of limestone, 81, 85, 167, 212.
Wellsville, rocks at, 486; sandstone and conglomerate south
of, 487.
Wenlock formation of England, 144, 152.
Wheat lands, 240, 261.
Whirlpool on the Niagara river, 99; ravine extending from,
388, 389; shells at, 403.
Whittlesey, Mr., report on the topography and geology of
Ohio, 23.
Winds, their effects on lake levels, 410.
Wolcott ore bed, 61.
Wolf creek, gorge of, 374.
Wood and shells in clays and sands of Lake Ontario, 317.
Y.
Yates county, rocks of, etc. 458,
DESCRIPTION OF PLATES,
PLATE I.
FossILS of THE MEDINA sandston E.
Fig. 1. Dictuolites Beckii.
— 2. Fucoides auriformis.
— 3, Fucoides heterophyllus.
PLATE II. "
Surface of the Medina sandstone, showing the clouded appearance from different kinds of sand, the
stranded fragments of rock and shells of Lingula. This is a common appearance upon the surface
of the thin strata over many yards in extent, and throughout a thickness of many feet.
PLATE III.
Fin and Scales of the Sauripteris Taylori, from the Old Red Sandstone. The fin is a little less than the
natural size, and the scales are of the natural size. The sauroid character of this fin is well repre-
sented in the arrangement of the bones, as seen in the engraving.
PLATE IV.”
Natural section of the bank of the Niagara river, from the falls to Lewiston. The successive strata and
their disappearance beneath the water are explained upon an inspection of the section. The water
level is carried on from Lewiston Southward, showing a depth of one hundred and four feet at the
falls, being the actual descent in the surface between the two points. e
* Plates IV, V, VI, VIA, and VI B, represent almost a continuous natural section from Lake Ontario to the Penn.
sylvania line. The low uninteresting banks occupied by the Onondaga salt group, from near Niagara falls to Black-Roſik,
and some other portions of little interest, are omitted, as being unimportant.
[GEoL. 4th DIST.] 87
678 DESCRIPTION OF PLATES.
PLATE W.
Coast section of Lake Erie, from Black-Rock to one mile southwest of Sturgeon point. This section
shows the succession of strata from the Corniferous limestone to the Hamilton group, with the lower
members of the Portage group.
NOTE:-The figures below the section in this and the following plates indicate the distance, in miles, from Black-
Rock or the outlet of Lake Erie.
PLATE WI.
Coast section of Lake Erie, continued from near Sturgeon point to the Lighthouse point at Dunkirk
harbor. The rocks exhibited in this section belong entirely to the Portage group.
S.
V
PLATE VI A.
Coast section of Lake Erie continued, from Van Buren harbor to Chautauque creek.
PLATE WI B.
Coast section of Lake Erie continued, from Chautauque creek to the Pennsylvania line. No rocks
appear upon the lake shore higher than the Portage group, but by ascending a few miles from the
lake shore the rocks of the Chemung group appear, and to these succeed the conglomerate, as seen
in the section across Chautauque county.
PLATE WII.
Section across the formations from Lake Ontario to the northwest extremity of the bituminous coalfield
of Pennsylvania, along the line between the third and fourth geological districts. The order of
succession of the strata from the Medina Sandstone to the coal formation is very clearly exhibited in
an almost continuous natural Section.
This section was intended for the Report of the Third District, but being engraved too late, was left by Mr.
Vanuxem for the present report,
PLATE VIII.
Section of Lake Erie shore one quarter of a mile in length, showing broken strata and intermingled drift.
The explanation accompanies the engraving. Numerous examples of this kind along the lake
shore show the effects of that tremendous force which has broken up the solid strata and moved
them southward. The motion of these fragments, with gravel and sand over surfaces still undis-
turbed, produce all the phenomena of striae and grooves which are often attributed to other causes.
DESCRIPTION OF PLATES. 679
PLATE IX.
No. 1. Section across Wayne county.
— 2. Section across Ontario county.
— 3. Section across Ontario and Yates counties.
— 4, Section across Steuben county.
The two figures above at the right hand are of alluvial hills. By uniting the sections 1, 3 and 4, wé
have a continuous section across all the formations from Lake Ontario to the Pennsylvania line.
The outline of this and the sections of the three following plates are at a uniform elevation above
Lake Ontario, and the numbers given indicate the height above that lake, in feet. The base of the -
sections is sometimes continued only as low as the level of Lake Erie, or even of Crooked lake,
These variations are all indicated in the engraving.
PLATE X. ^ -
No. 1. Section across Wayne county.
— 2. Section across Seneca county.
— 3. Section across Tompkins county.
— 4. Section across Chemung county.
By uniting these four sections, a continuous one across the district is presented.
Section of the inclined plane at Ithaca. The letters a, b, c, d, &c. indicate the numerous alternations of
hard and soft shale and shaly Sandstone, with a few courses of compact calcareous sandstone.
PLATE XI.
No. 1. Section across Monroe county.
— 2. Section across Livingston county.
— 3. Section across Allegany county.
These three sections united present a continuous one across the district, along the Genesee river. This
section shows the succession of strata from the Medina sandstone to the Old Red Sandstone and
Conglomerate.
No. 4. Section across Orleans county.
— 5. Section across Genesee county.
– 6. Section across Cattaraugus county.
These three sections present another continuous line of section across the district. The relative eleva-
tions of the surface are continued throughout.
*- PLATE XII.
No. 1. Section across Niagara county.
— 2. Section across Erie county.
— 3. Section across Chautauque county.
The three sections united constitute a continuous section across the western counties of the district.
The two outline sections, extending from Cayuga lake to the Genesee river and from thence to Lake
Erie, are constructed from actual surveys, and present the elevations of the principal hills and
valleys. The elevations here given are from the tables accompanying a topographical sketch of
New-York (Transactions of the Albany Institute, Vol. I.).
87° -
680 DESCRIPTION OF PLATES,
PLATE XIII.
Section 1. Natural section along the Genesee river, from Mount Morris to Portage, showing the Genesee
slate succeeded by the rocks of the Portage group.
Section 2. Natural section along the Cattaraugus creek, exhibiting rocks of the Portage group.
Section 3. Section across the formations from Cleveland, on Lake Erie, to the Mississippi river.
This section commences with rocks of the Portage group, and shows the succession of the Che-
mung group, the Conglomerate and the Coal measures. Descending to the southwest, we pass over
the same formations, which are underlaid by a black slate, resting on the Corniferous limestone of
New-York. The Corniferous and Onondaga limostones are well represented; and below these we
find a drab-colored soft limestone, which is followed by a continuation of the Niagara limestone.
Below this we find impure arenaceous limestone, and thin-bedded limestone and shale, which show,
by the contained fossils, their equivalency with the Hudson-river group of New-York. Following
the section from Cincinnati Southwesterly, very nearly the same order among the strata is observed,
with the exception that the Chemung group is separated from the Conglomerate by a yellowish
grey sandstone, with thin beds of oolitic limestone, and above this by thick-bedded grey limestone,
which increasing westward forms the most important limestone formation of the Mississippi valley.
This limestone is followed by the Conglomerate and the great Illinois coal-field.
Section 4, Section across the State of New-York from northeast to Southwest, showing the natural order
of succession among the strata, from the Primary upwards to the Conglomerate of the Carboniferous
System. By uniting this section with the one above it, we have an almost continuous section from
the northeastern part of New-York to the Mississippi river. In the space between Chautauque
county, the termination of this section, and the commencement of the other at Cleveland, there are
no rocks seen, except those of the Portage group.
PLATE XIV.
Surface of limestone, exhibiting furrows and striae. a, c, e, f, g and h are nodules of hornstone. At a,
c and g, these have resisted the wearing force, and are elevated above the general surface. At e,f
and h the modules have been broken off, so that their surface is now lower than the surface of the
surrounding stone. From a to b, and from c to d, there is a little elevated ridge of stone remaining,
which has been protected from wearing down by the hornstone before it. It will be perceived that
the striae are often convergent or divergent, and that near the bottom of the plate there are two
which are curved and Suddenly terminate.
PLATE XV.
View from Bigflats, looking down Chemung river. The hill on the south exhibits numerous gorges,
or incipient ravines, which are annually deepened by the action of frost and water.
GEOLOGICAL MAP. 681
PLATE XVI.
Ravine at Hammondsport, Steuben county. Rocks of the Portage group. This is a common feature
in the scenery of the southern counties.
PLATE XVII.
Hector falls, Tompkins county. This waterfall is almost directly from the top of the cliff into the lake,
the gorge being worn back but a very short distance. Rocks of the Portage group.
fºLATE XVIII.
Lodi falls, Seneca county." This fall of water is over the rocks of the lower part of the Portage group,
at the head of a gorge three-fourths of a mile from Seneca lake.
PLATE XIX.
Deep gorge of the Genesee below the Middle falls at Portage. The cliffs below the falls are of the
rocks of the Portage group, three hundred and fifty feet in perpendicular height.
GEOLOGICAL MAP OF THE MIDDLE AND WESTERN STATES.
In this map are laid down the limits of the principal geological formations occupying the States of
New-York, New-Jersey, Pennsylvania, Delaware, Maryland, Virginia, Kentucky, Ohio, Indiana,
Michigan, Illinois, and a part of Wiskonsan and Missouri. A portion of Canada, bordering the great
lakes, is also added. The accompanying table of colors, and the sections 3 and 4, plate XIII, will give a
correct idea of the order of Succession among the principal strata.
NoTE. The first intention in constructing this map, was to show the extent of some of the New-York formations be-
yond the limits of the Fourth District in a westerly direction. As the work progressed, new materials accumulated,
and a tour over the western States offered an opportunity of presenting the unbroken continuation of many of the New-
York rocks as far as the Mississippi river.
In laying down the formations upon this map, the annual reports of the different States furnished valuable data; and
although I had travelled over the country in different directions between the Atlantic and the Mississippi, and was well
acquainted with its general features and the outlines of the more important groups, still I should have been unable to
give the exact limits of many of these formations but for the kind assistance afforded by many of my fellow laborers;
thanks to the enlightened and liberal spirit, which in the free communication and interchange of information has so
rapidly advanced our knowledge of American Geology: and it is with pleasure that I acknowledge my obligations to the
* By an error of the engraver, the plate is printed “Lodi falls, Genesee county.”
682 GEOLOGICAL MAP.
following gentlemen. Dr. David Dale Owen, the State geologist of Indiana, has permitted me to copy his maps of that
State and of Illinois, Kentucky and Wiskonsan, including the lead-bearing region of Iowa, into which his researches
have extended. Dr. Houghton, the State geologist of Michigan, has obligingly furnished me with a geological map of
that State, where my own observations have not extended far beyond the lake shores. In laying down the formations in
Ohio, I am indebted both to the reports of Dr. Locke, Mr. Whittlesey, Mr. Briggs and Mr. Foster, and to personal in-
formation from these gentlemen. The valuable paper of Dr. Hildreth, in the 29th vol. of Silliman's Journal, has also been
of great service to me. In coloring the map of Virginia, Mr. Slade, a member of the geological corps of that State, has
pointed out to me the general limits of the formations in the western part. Prof. J. T. Ducatel, the geologist of Maryland,
has kindly furnished me with the outlines of the formations in that State; and Prof. J. C. Booth, the geologist of Dela-
ware, has afforded me the same facilities. To Richard C. Taylor, of Philadelphia, I am indebted for a colored map of the
eastern part of that State, recording his own observations previous to the year 1834. This map shows very minutely the
position and extent of the detached or outlying coal basins on the northeast, and the eastern limits of the great Alleghany
coal-field, Mr. Taylor has spent many years in investigating this region, and particularly the position and extent of the
coal-fields, and no one is better able to give the geology of this portion of the country. - - -
The numerous and frequently alternating strata along the eastern margin of this great coal-field, as well as of the form-
ations farther east, could not be represented on a map of this scale without going into an extent of detail incompatible with
the present object; in many instances where two rocks are colored alike, they are marked by letters which will indicate
the formations by referring to the corresponding letters in the index of colors. Bordering the Atlantic south of Dela-
ware, one color only has been used, from the impossibility at present of giving the exact lines of demarkation. The ex-
istence of some minor axes within the limits of the greateastern coal-field, and the appearance of lower formations, have
not been noticed on the map, as their limits could not be accurately laid down without a more minute survey than I have
been able to make. * After leaving the western extremity of Lake Erie, the Niagaria limestone, the Onondaga-salt
group, and the Helderberg limestones are so blended that it has been found impossible to define their limits by the same
colors as in New-York; the blue, indicating the latter series, is therefore continued as a representative of the whole
through Ohio, Indiana and Illinois. The area colored of a deeper blue, with a margin of slate color, of which Cincinnati
is near the centre, represents the Birdseye and Trenton limestones of New-York and also the equivalents of the Utica
slate and Hudson-river group, the latter having become so calcareous that it is known throughout the west as the Blue
limestone. f The purple band, indicating all that remains of the formations between the Corniferous limestone and
the Portage group in Ohio and Indiana (the black bituminous shale), represents these as terminating before reaching the
Rock river in Illinois. It is possible, however, that this shale may be traced farther westward, although it was not ob-
served in my examinations along the Mississippi, - --
The difficulties encountered in completing this map for publication have not been few, and I cannot flatter myself that it
is free from error; I appeal therefore to my friends and a generous scientific public for their forbearance, hoping that some
future opportunity may enable me to offer it to them much improved and corrected; and in the meantime any information
or suggestion will be gladly received. A geological map of the remaining portion of the United States is in preparation,
and will soon be completed. This map will exhibit the limits of the principal formations east of the Mississippi, and be-
tween the Gulf of Mexico and the Great lakes.
In the present map the wide and almost undisturbed range of some of the lower formations is well illustrated, and the
immense extent of the two well known American coal-fields seems almost incredible. The great Illinois coal-field occupies
a space nearly as large as the whole of Great Britian; and the eastern one, occupying a part of Pennsylvania, Maryland,
Virginia, Ohio, Kentucky, Tennessee and Alabama, is even much larger, occupying an area of sixty thousand square miles.
These vast formations, with associated iron ores, prove the existence of those sources of wealth, prosperity and civilization,
which invite to enterprise and reward with plenty. Although not strictly appertaining to a survey of New-York, she is still
not an idle spectator of the vast possessions of the west; she stands upon the vantage ground, and the great mart of the
Atlantic is only reached through her lakes, her rivers and canals. The immense territory north of the Ohio river, occu-
* Since this map was engraved, a geological map of the western States has been published by Mr. Byrem Lawrence. The main features of the
two maps are in accordance, but there are some points in which I have felt authorized to differ from Mr. L. in regard to the limits and extent of
£ertain formations. # See Chapter XXIII.
GEOLOGICAL MAP. 683 *
pied by the same geological formations, possessing an equally or surpassingly fertile soil, is straining every nerve to throw
her productions into that ocean thoroughfare, the chain of great lakes; and if New-York now feels the influence of that
youthful country, what will it be when the populations and productions have increased to ten, and even twenty times
their present amount 3
To the geologist here is a vast field laid open for investigation. The unbroken extent of strata offers the means of
tracing over wide areas the lithological changes dependant on deeper waters or greater distance from land. The fauna of
this ancient ocean presents great and interesting changes, as we progress over these wide districts—its ancient bed.
Changes, both in organic remains and the condition of sedimentary deposits, are constantly presenting themselves; and
when these shall be more fully investigated, we shall feel at liberty to draw more general conclusions, and to propound
more comprehensive theories respecting the primeval condition of our planet,
ERRATA.
Page 19, for “VII,” before quaternary system, read “VIII.”
Pages 39 and 48, for “Pleurotomaria,” read “Euomphalus.”
Page 59, 13th line from top, for “amss,” read “mass.”
Page 97, 12th line from top, for “Plate 3,” read “Plate 4.”
Page 107,
Page 113,
Page 117,
Page 118,
Page 122,
Page 131,
Page 133,
Page 158,
Page 172,
Page 175,
Page 189,
Page 195,
Page 200,
Page 205,
Page 206,
Page 212,
Page 219,
Page 224,
Page 257,
Page 280,
Page 285,
Page 315,
Page 327,
Page 340,
Page 352,
Page 406,
Page 481,
Page 503,
Page 509,
Page 509,
1st line, add “Spirifer sinuatus,” before Silurian Researches.
for “41,” No. of woodcut, read “41 bis.”
2d line from bottom, for “one of the most important groups,” read “the most important group.”
4th line from top, for “Mackinaw,” read “Mackinack.” .*
in explanation of woodcut, for “a a,” read “b,” and for “b,” read “a.”
13th line from top, for “place,” read “plane.”
16th line from bottom, for “geological,” read “sedimentary.”
18th line from top, for “specimen,” read “specimens.”
16th line from top, for “2 a,” read “6 a.”
9th line from top, for “3,” read “4”
9th line from top, and page 190, 8th line from top, for “Delthyrus mucronatus,” read Delthyris mucromala.”
8th line from bottom, for “Dimyaira,” read “Dimyaria.” *
in explanation of woodcut, for “Loſconema sinuosa,” read “Loſconema meavilis,” See description of same, p.201.
in explanation of woodcut, for “Orthomata,” read “Orthonota.”
10th line from bottom, for “pressed,” read “perfect.”
illustration 190, the strata beneath the Tully limestone are incorrectly represented as horizontal, whereas they
should follow the curve of the stratum above.
13th line from bottom, for “Seneca county,” read “Seneca lake.”
reference to sections for “Pl. VII,” read “Pl. VI.”
15th line, for “plain,” read “plane.”
2d line from bottom in note, for “right hand.” read “left hand.”
10th line from bottom, for “rock itself,” read “rock in situ.”
Catalogue of Mineral Springs, 4th column, 8th line, for “Cal. Mag.,” read “Sul. Mag.”
14th line, for “the accompanying plate,” read “Plate XIV.”
13th line from bottom, after the word “thrown,” add “down.”
10th line, after “opposite,” add the word “side.”
13th line from bottom, for “northward,” read “southward.”
8th line, for “birdseye maple,” read “birdseye marble.”
7th line, for “the same as fossils at,” read “the same fossils as at.”
17th line, for “were,” read “are.”
in note, for Tenestella, read “Femestella.”
P. S. A few hundred copies of this map were colored, showing a narrow margin on the north and
west of Lake Ontario, in accordance with my observations as given in the Annual Report of 1838.
Mr. Logan, the Geologist of Canada, has since examined the map, and expressed not only an entire
willingness, but a desire that the portion of Canada now colored should appear on this map; and I take
great pleasure in expressing my acknowledgments to Mr. L. and his assistant Mr. Murray, who have
very liberally furnished me with all the necessary information. I have the more reason to express my
obligations to Mr. Logan, since his map of Canada cannot appear before the public in some time. By
means of this information, I am enabled to present the continuation of the New-York strata through
the peninsula of Canada West, thus showing their connexion with those of Michigan on the northwest.
Prof. Fraser, of the University of Pennsylvania, has also given me much additional information
upon the geology of that State, derived from his personal observations. This will be of essential aid in
correcting the details of a portion which remains uncolored on the present map.
ngitidul
- L- --~~~
-
--~~
E BOYo AN:
r-------------
(F) rulu giral Allap
of the
WYAND OT
-
-
-
-
-
H sº iſ ſº is LE
---------------------
--- - ------------
chro
º
NAMIC KEE
- º
- - - - -- º -
& /~ & /
ſ sº e - , , , , sº o
- ºw- - Walo.” C 1. º
- º - ^2/ - - Plorºº
- -
- ſ º
------------ - - - - - º º … º/, -
--- -29 A &^. *º-
AD A \. - ºf ~/. - - -
| º - -
Nº win g on
T-
- -
º //, // > Fº * A
-
º
º
__
assieux
º, to -o- * 0. +0. ºo: -o-, *—º-
--- - - º º
- º - - - - - - - - - - - - - - - - - - -
Scale of Statute Miles º tº | /
| | |
NEW
Aya
O
H of E D iſ ºn T. N. E. W. Y O R. K.
CO STA
*
|
- Pºkorra. |
zºon tag,
|
D
|
ºtſ/cºa/, ſ B. A R Rºº.
º 'º-º-º-
º was -
| | | g RAT I tº ºr º 'º º'º
) º P. J. - -
- ( M. ſº / T- ºf º-tº-2's
º º N. T. / 2. ... . . . . | º N - g º N Esº - º
—“”º \, . – º –- Lºs - ?---
| - \. -- - - - - - º, .. - |
- -- - - - ſºon º |
Sº C - - * -
" " ºr --~~~~ || || 3-2 Sº I º -- " ------------~~ -- " - -
- - - Atticº º- º * Pº------ - \ - - - - Q - º ! |
- H - . … o N - - - - º |
RA of Nº || \, jºſſ' . . . . -------*º-º-º-º-º-º-º-º-º- Zºº 3 day º º * - - - &
ſwallwo RTH - OA. K. L. A. N. º E wyo MING |}^ 3 4 », ſº º 'º. Nº --------- e. S., / º Yº -º- 2, -- - |
- LIV NGST DN Macomº - s __ -- T !, *…
º º º ºrºa. | - _º - Zºo º ----- - | ---
Zoºey/ º
I
-
-
- - - - -
/ / […" , , , , ºr ºl. Nº º
º ) ...sºs. y º G. R. E. - ... ſnººn
º - zºº/ſº sº
- º -
º
-
-
-
- Jºzº
-- --------------------- sº 2 - o º -
T ------------- T--------, --__ WAYNE- º º * * s T E U B E N - O y - º -> …
- º - B. R. º: ºnton . -
--
. -
- ---
A L L E G A NY º
s: A - ºr tº a
tº
º s º -
- º
º
C AT TAR AUGU
º H-- - -
-
- - -
- -
- ---
- -
-
-
N* - - º - º 1,2 n.,..., ºf
A. º An I ------ - | - N // % - - """ - * - º s sº º º
#|s *on º - - |\\\\ ºr - º - */
i. - º -
º, ºr sºngston "
yº
Tº a ſº | | *" ºf Iº- || A/ N A 7 jº-i-º-º/~------------------ Yº sº ºf // | * ºf cº / \ . . ._____.
Yºº ---------------. DERA, ºr , , , ) | * 00 RA 77 sº-º-º-º-º- ºr ~ Zºº 17, \!\!\ ^% g ºf ºil------------------~~~~ susaur. HANNA
*Montrose º * / lº
ºf
ºr/erººrº.
º
-
po º º R.
-
- - - º --- -
D -
ATINr.”
togºning on -ºº
º SLAND A chº - º | 1 *
| H. E. - -->
L.
| Anz, -
"º
ºr ºl, STRUHEN
ºrbºrg
zºº.… GEAU GA
º:
Nº"
* ºn --
Pb RTER -º-; |WILLIAMS ---------|------- º !--. - -
º, ME R C E R ! | - oneon FOTTA) º - º
- º - R ST º R R - Armora, ------- - * s - --
º A. º ſ - - - | - - - - - - - - - Sº,
º " ** º o º | SAN) o C UYOH O GA ºf - º º º º
| | MARS I - RY - - . - - - - -
º º ºran’ \! - W O O I) Zouer. Eº . - | º 2. jº. |- º º º º º º -- -
--- - ºr. POR ºn , , , º/ "Oºº --
- | | | | * * *** M A. R. A. ------------ - * > Lºº. ... ... ---- Tºº-----------|-- KDSCIWSºo ! * " i ∈ - ºccº cºlº A RFIFº º º º %
- iwi, --- | - C. L. A R. O. N - 2 . s - º: |
WHIT -- |-------------------- - Zºº, º * - ſº ºr- lº -
-- o ºf- º - º - - T --- * > - -
S E. N | - = - º - - º ºver ſº r/fºº, - . sº ºs - -- - -
-------------------- … º g- E. ºrnbºrº. - sº y - * --- *— ---
º, ºu Nºrºo Nº. * > ***, ºf "Aw
ºw I ºf tº sº - ºn º º
NAM HAN c dox c RAM, FoRD ºw,
wº. Manºeia.
| | | RICHAND
- - º º' --
... - º º ºº: -
Aitenº. UN PDON :* * º * º
-
ARM/STRONG: : -
º º º
2.
IN º
-
…
wº-
O
º,
º
º
4.
-- . . . . . . - … - … i - - - - - - - - - - - - - - - - - - - - - -n_- + 1 - 1 - T -------- tº i v - 1 - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- Lºza,
Zºgº He F. A | - º -----
º - - ------ || |Bº NT \ ---
º -
* º I S | - --- º --- OLL | ------ - E. N.
º | H - - - - - - - - - "… Nº |
Y - -
-
-
---
-
M
A.
N
|
| - .." - º Nº. Nº.
ſº H …sº
- Fºw E L L º ſºara, Že --- - - - ºº: - sº _º -
- - - - - º Prº - - - º- _ - º - -
º - - - - - - | - º T - º - º - - º
º | | | º | | W.A. R. R. E. | - º º G. R. A *kroº º - º º º - º, º º | º ºf . º | º
º -----------__ ºr ------- - - - º * I. ºf - - - --- - --- - - . . . . I, nºr- … sº -
S. C U Y.L. ºn 4 - | º - TIPP º J/º * I TUS | | | º: : C. | º, * W. E. S. TM ORE L.A. - **** … - s
º K N O X ſº shoc to Nº. º, º sº º - º º | _º|10
- ... ºr ºf O. - - -º- "". Aſ ºf A -------> \ \º---------- º | º | - Fº º - a N. C. - |
| "Lº NAR. In º' T-' /* , º , a e º 2–1–7 U. N. : \|^ Y, "ºº-ºººº ſº... . . . N. H. H. Lºſ Hº Y TTT 1-ºctºr’tº | | | | `--T) A HARRISON = ſ/º. º. L AN º s -
H. - - ºn-º-º: - -
R 0 wºv | Zºº, - ------------- nº - --- º º º --- *
º M ſ | º LV. º/ | º º ºny - - º -- º | - 2. C - |
|- ſº - - . 2,…,’ º \ - º, ºr lº -
| º R G|A N | - - - - - H. |Sº GUM * º º MONT T. * - - º º - - s º * Yo | º º 2 º º *2. º |
ºf | - - - - - * * * * * - | EV/º'ſ "'º | K"> /* Iº....., x. 2. º || ||
ºrº - + -º-º-º-º-º: ---. … - - ºf) A M * - º L/ . .” - ESTER º ". || ||
2. º º, - l ºrºgºeza X GUERN SEY sº … . f ºf F OR D / N. KL INº. ºY R. K. 2. ſºot Cº >\ ^ 4 × | -
I’I K. E. SC ºn Tº | S. ANGHAM |S º | º Z. ATYNE T----------------- C L A ZººZºº º - - | *: º ". | - º - ºrg/ - ... ſ.l.. . . .- E. . º - A/
- - - ºw. - – "… - A. - - , | == ºſ-------------~~ -- . º
ºzº ºz. . . ". - Łºzºa. Montgomºkyrº- nº º * ºr nº Aſ | ... ------------ ––––ºf *4, 2. º.º. " *72, º//
-------. º ºn G. - || P.A. R. º º ºtiºnſ) º - - #’RE B L E. | * º | - ºn º - ºl. 2. º ſº | -º-º: -- - º º - º
r- --~ A. R. º | o --- -----4---~~~ * Tºjº- Mio N. Roº, 5%. --- ºn- º, Zºº º º / ºg 2.ºr 2 ſº
D. A N. º S. º, I E. - º - AM º - - - | - * - º - S. - * º _* º - º A.
H E Lºº Yº -- | - A - \\ . | - - - G- al.,... - M. O. R. G. N. --> -- 2 // > - 3\º C tº - 2-
º | | | º º - – º, - MO R (, - - - _______j --------- ºv - | - tº Y L. E. R. º º º s - º **** --
* --- - --~~ | - I º | " | - - * - I - || 2 | "T" - - - - º, - - - ſº - º - - -
- | - - º, - - - - A. º . - . - W A S N. G. I O Nº. - - º º ºt sº - --~~ -
A * | ** A R R. º º, H----- ºiſe "LINTON: ...º.º. Madº - Sº ſº. 5 * º - ºs
| ºn--------- - I Gº O ºpen ----------------|-- / / L. - - Mºor, - - ºſ ºf . - § " * \ º º Zºº ... º.º.
- º Dºº- - ºr º - - --- - - Zºotº - § - -
tºº. * | | - -------- | |O Wºº DE CATUR … s. - - |\, . - ºs- - ººrtºn º - º - º º - e - Rºs º
30 \,. LIN C OL Nº º * | _º -- / . - | - &zerºwry * ſº º: --- ºf - H. E. N. S. -ºººººwº | ºn ARR --- * / º - in is - º s ſ? l, Aº, ºf º - - - \\ º º al-
| º | ºf ------------ ": 2- || || - º ſº ſº" ſº y º 'º' A. ... ſºon TG-OMEBY }-\º * , º Nº||
- A.Y. T T. E. ºre. NG. J.A. º *AN \\ () D º - º *g AV-7- * º - - --
| --- 2 ºr
º
Hisºros
º
º tº __ ! ---------
\ º - --- __
sº sº. 2 - A º
- - - - - - - - - -
--- - - - - - º º - - * … º º - sº - D O
* * Z ºf , º, ſº tº
- - - - - - º -
ºra **
-
-
º- - - ---
* ºpy, HEN LOPEN
- -
----- MAD IS o N. * 9. -------- - * . . . . . - º - º
- - -------- - - - H - GS tº Y. LA/ º º I. - - º º, |-- º X. - C
--------- - - - - - - - º - - º º -
| º º - º º ºf 5 ºf Aºk so N. º º W. - º * .. ". º sº 2. *
- - - | º - - | | | | | - º º * - - - º, º - º º N - " - º Aºr/ºr * - - - ºt. , . . .
- - wº | - - - º . - - - - -- sº º S. ºf . - X w Zºzºy.
its 23, Zºº sºloa. - - - - - L^pºſłREERSONSWITZEF ºws ADAMS º * " ...? º, º Aº 2," º * ... º. Sºzz
º - º -- - - - - - - - - - - - - º - - - - T- º - - - - - º - - "... - ... - º
- - *gºroº ºf | Wºº ºnion --- | M. A. W. O. N. º º º * º, º ". w % wºreezz
- - - - º
º - - - - º º - - - - º - - ſ -
- BRAX T O º s sº Ali. º º º - ºf , º, º 2. - --
º º º - º º º ſº ſº # º º, º º - - - * - º' ) Q ... -------- u | | A2, A22 Szyzz's/ozzº
- - - - ººº- - sº º º -º'ſ ºy º º
---
ſ
ºf Awºsº. A
-
-º- an
--- -
º, ºngº - º: S.
-
º
º
º
- º
- | º).
tº º - -
º º º _* -
- - | º-s, -
Wºº (7.4%; ſº * \
- --
-
| | , sco ºr º -
\º ºf T- - - --- - - - - - ºn, hº º - - - -
- " - " -- ~- - - - - - WASHINº. - - - - - º . . . . . . -º/* - A/ºzzº
º, ºl. Ashington ... º; K). nº * A 3.92; J, E W I - º, t º
******* ºr ºº - º ( , " … . . -- - , , º 2,
º' 6 tº . /... [ ] **
- - * G. R. E. E. N. U P - - -
CRAWFOR Fºo YDº! / S Maſºº H.A. Rºſso
... G I B so N ºn tº or sººn º/ . –
- - 4. -
º
º º r *zozº Zººes”.
º/p | - |*** Szyzz'ºoze.
º/ o | ****
Zzzzzzzzzzzzzzzzzzzzzzzy
n ſº Søe.
Zºzzzzzeszozzeº,
n zººsºozes
I | ºzo.” Sºgºzzº
k | |Mººº. &^*
i | | ºzºzzzzz zºzzº
h | | w. Szalº
ºr ºve 5%zºzzº
ºn 1 ºn o 1, A S
- *
- - - --> º P. E.M.A.L. E. º º/7
- - 7 Žººſe
º ºrie L.
* - - - - -
Lºs C o TT * *
- *
º ---.
º º
º
38
- ,
º
ſ
- ſ
- ºf Z.
º º
HARRisøNº||
º * A
Yº.
-
-
|s H E 1.
* *
L-º-PTSN
, sº º,
WASHINGT KS: GENEVIE
POS ºr
-
-
-
-------
- - -
…'s PENCE 57.
PERR
PENCER
ſº -
- * -77/7 . º º - -
--- º º M. º
Nºjº -
ºr tº
-
- -
-
|
Nº º Pºzº.
º ſ ºf Riº KENRingº
-
- - º º - -
AUNION U - / *
ºn H A R DI Nº. -
--- - º
º º
º,
WILLIAMson: CALLATIN
º
ºnosº
ſº.
º º
º:
TTT ------------ - º Jackson - º -
.
S.
-
Z' MA D SO Nºr;
º
*/
D. H. L. O. ſº R A Y so
- - .
º, (2/22/2”ze.
| | Mºzgaz /ºzz-e-***
- | | Z/2Zazz Szczze.
Aſſºzzºzseye zºzz
d Zºewºoz Azzºzeszoºes -
c | ] zzzzz/2 ozzº Sºzzº.
b | Aºzsaw, sazzºzozze
º | ****
Zºº Aawaz
-
º
º
ºf
ſº R.C.
º
º
-
-
--~~ … ºr .. { fanzº. --
H. O. P K I NS ---, -º U. L^ \LIN c of
- º - - - - - -
ſº ºº | º, C. R. E. º Nº. |Zºº º
-º- º - cº, *
º C[A S.A., º ---
2.… Nº 2" * . . . . . .”, ºntºrow
- - ELL - - C. H. |NOTT
- -
- | - º - - - - - - … º - - - - - - - º - - -
* FNR A - - º - - - - - - - - º º º - - - - - - - - - - - - - º, º: º - - º
- O - | º - - - s S. º - *. - 2. º/º - | -
- - - - - - - - - … - - --- - - - - - --- -
H - - - - - - º - - º - N º S. - H - - º º --~~ / º º - -
- - - * º * º - º º - - | - N ON−). #4 - º |||ſ - º'
- - º XIrº - - - - sº 2-M. Lº / ; In º sº Zºº" " (". *** - & ºººººººº. A ſº ſº,
- -- - º º | - º º - - - - - - - - - - - A- – - - - - F. - | ºl. - - - - º || ||
- - - º -n. -III - º
- º 5... - - - º - N. - - º *º. -- ~~ º * ..., --~~~~
- - -> → - º, - º º - - - - º - - - s - º - - - - | º - -
- - - º, - | º - - . - - º - . - - º *. - - #. - º - - - º - -
- - y Z/º is - - >< ºf º ". . - - -º-º: - º - s: ſº º 'ſ
º º - i. º - º - - - º," - - C// . . . ºº: º
º- - - - - - - - - - -- - - - º - - - -- º --
- ". - S T o º º º º - º - - - - º º - - - - - - -- - - --- - º - A º - º: \ º - º º
- OD D. A. E. D - - º --- - - ºn 1 m ------------ ------ -- * - 2. ". - º - - - - -- tº - - - - - - - '*' - Sº - D F O R D/CAME - D LE - R. R. Y. - º - l, Nº sº -
| Bl - º- º/ - - - - - - \ --- Z. wº ^ - - - º, º, sº - - -- - is, - - _/ º o - \º º .
°ºgºſie - Nº. - - º º º, e. - - . - - --- º º %a) -- / - | N. º º | º º - ºr - -- º dº. - - S. º | tº - - & º º - c - - - - -
º º º- º, (Zaszow D AIR / L.A. , s , -- º º º 'º ºf º" .. *..." – Zºº gº º * Nº -
| ſ - -- - º . --- - º - - -- * I -- --------- º º º - - - o - - - - - - º >\ ^ Aſ. it! - º S S E. X IS |E of wiGH º ". -
- sº..…+ i + zºº wº ---, - f{ISSELLys -- - -- º' - "N"º - dewºton Zºº º ". ºf-
- - - - - . - -- - -- - -- - - - - - - - -
- º º _ ºr. RREN'ſ - ------- - - -- . - º A - - --- | - -
| - - - - ". - - - - --- - ºn-ſº - - - º --- -
- Cº. Law - -------* …" - Lºr, - - . - - - - º 7. º - - º ºn cº- …” … . -
|J. o T R G G | * *. º A. N. º ºcota, - e. . . / - --- º WY T H E – º ---, -- º "A. º – Kºº * /ø aſ ſº º ---
- - - - - - - º - - - - --- - - - - -
dr \ º | | SIM SONº. …” - º - sº - . - º --- - º º 'º -- **---- º º "Aſ. - Borºzon - - Kº, ºf º |NO R F O LK ---
Mew Madrid – ºr º . . . . ) … . . . - - ºn ºf º º * \º T---------- - o 21. - r - -
- º 4-sº **-*-----_ - */AL LEN KMON RO in M. - - - . . . . . . . - º ſº. º' - lºs ºs he n a y "* YLVANIA, HALIFA X o - Hickºº souT **** \\
º ºf - - - ---. - - º, - º º º º - º ºlº - - º º -º- - - ºº. H.R. - - º - W
Wºº---------. "T"------------. . . \, - - ºr ºf ºSHIN ºf Nºt Ridkº.º." Yºº AGREENS VILLE X------------------'Tºº
º "T"------. - "T"--------------. . . . ºº!º º' --- tº ". sº sº sº. Markarºſe - º ºrkºw . . . . . ------------" º
lº- - - - - - -
:
--- -
ºt.
cºlº,
º
G/
I. |_ tº Zzzaszowe
7.5 ° 7 * *
- - - - -_ - - - - - - -
- - - - 82 * 7 O =
-
-
-
7
&
-
7
7
-
STATſ E.S.
N
- |N
lſº
£S iſ F.
.
# AND Wy
|
{D} {}
|y||
A P of THE
W
：
G |CA|,
T
\
{}
ſ
A
S Expº ANATory of A GE()
|N
|N
SF.C.ſ ()
4/*?）?）? OZZAVºz, Zz
|
|
*«??????«/«/ sºoºoººº...«|
|
- ------|
JºA!!! ºù Baeſº (I
ºººººººº ºzzzzzzzz)
ººº^ºº«27 zº zºzºzº
！7
taſ
·
|-
ººººººººººSº ººyae，
|×
ººº， 22%， zozzzzzzºzzº
}^^
ºººººººººººº«øszą，
º^^Xººº«27-2，272，24 Z.º
ºººo..ººº^^^^^^^^^&???，ș
•^a«» ， » »，
**;
ºoºº，)ºzzzzzzz)
^^^^?%22&zºº 222/22/2)
Źº??7Zºº ºzzzzzo，
*： ：
• 0
ººzº ºzzzzzzºzº ſº
ºoºº，)«ºzzzzzzzzz||
'aºrozºZºſº»/ºwo，
ºozº zzzzºzzy. !
I |×
ºxazºezzº ożywº，
ſoſteſuo eſſet}
ruoan Hºſ
|
|
|
ºoºo，) ºſzzzzzz
zvezº zºzzzzzzºzzº |
... .2/z c 4 2 a z Ço a ZZ” e //
ºººººººº« ^7. ºzzazzzzzzøy.zzz！
ººººo..º ^ºzzzzzzzzz！
zºzzº ººvaezo y
%%Zezzeszone.
e.g. Zozzeº,
y &
Zezzeróez:
A%ayara Z. zz
Zºro
awe,”
Z'rez, % Zzzzeszozze &//aaºoze
ſºwozºwezzº zºzºwszą z \，
ſaaaſae uſºuooºſſa. Jo ſmo W.
15% (7/04/ /*a*, *e 47/.4/VZ"/C (26/24/V aº Z///zz/or//zo/AAZ, OAZA/P/o za z/.../ 2//e *4/ara Zºº’er.
//Z, S'C' (2/V, SYZAV AP / / / /*.
o/
///V/PO/W Zo // e M/ozz//
SA/C 7/OAV /?oze the Sozzº e 222 of /, A / //
ºººoºº zawºwºgaeº，
.tº№TO/)odzwrºwyſ
Ķ
|- -&
ſeg ºxeadesøųO
^~
Ķ
ºù
S || || .
£
| || O
'deaſ opuſ040,4§.
）
ºſoaz ezzººoººº zozºwezzy?
*«ºzºzzz，222.2��4，
ººoººº«««««^) | $
~
^^^^^%22&zºº zazzº&2& & \，N
|-# ~ .
C：
ºz，47822427 zºzzzºſzŠ
?
ſuxºſ
！ 1
0
ºzazº zzzzzzzzzzzzz
·&ø.49ŹzºzzzzzzZzZſy ºzzzzzz，
ºººººººººº zºº， zºº.
ºzzzzzzzzºzó： \
ºººo，) zozzzzzzzzzz
ººººººººº«77 &ø7，797
ºzzºsºzzzzzazwºwy,{^
|-
º
///ße Zºmestone of Zºo/
Z/…sorº Zºver Grozzº
'deaſ H oſťO
- ºzzozººzzzzz zzzzzów，
ººººººzººzzzzz 4：2，727
º dºzo zº zzzzzzzzzzzzZz
dºzozº ºżzzzzzzºzzº
ſºzzº23'22427ºwozy，|
ºzozºzzzozóſzó： \ ,
Ó a 2 /
/ / / z. z. z z &
(
da Ayyſ iddyssſssſ.w.}
- - - - - - -
ººººººººzzzz 7.¿¿ {
Cincinnati.
A 7' / / / / / / C // C // A /V
ºw. Rºver.
A Z / / / /P
, ſ/ / ,S' ,S' / .S. S. A /* /? /
// e
Zo
Zºzy
af // e /z w are
// 2
AS’ A, C // O AV /r/, /
Zzrº or Aººsaſtrozz. Avrº
PLATE I.
F (" () IDF, S ET; R (). PHYLLUIS . F UC OIDE S A UER IF OR MIS
///, o/, //zazcoz.
:
º
º
---.
º:
º
º:
º º
º:
º
& º
s
NS
s~
ă
f
- Niagara -
Group.
Niagara Shale.
Red Sandstone.
Sandstone. -
- Clinton --- - - - - -
Group. 1 ºr sº
Medina
|
Gray Sandstone
§§§ºly -
* * *
NATſ (IJ R A 1, 3 g (D, T J D NI from L E W J3 T (D NI
HORIZON TAL SCALE
VERTICAL SCALE V2 IN C H TO
Niagara Limestone.
t(ſ) N J A D A R A F A L L = .
100 FEET .
PLATE IV.
ºr sº-º-º-
**
River level
-
--
Bloody Run.
***** at River.
- - - - - - -
- - -
G D A 3 T 3 E G T J D N D F L AKE E R J E from £3 L.A. C. K R D G K to 3 T || F. D. E D N P DJ N iſ. - PLATF. V.
// e Zºmºers zzyzoz &e Seczzozzs zzzzzzczze &e &zszazzae zºº. 722/es from Block ſtock.
Black Rock
Buffalo City A.
º
--- - - -
º fººt sºiºi__ - - -º-
- - - -
--
- - - - -
- - - - - - - - - - - - - - - - - -
eac/ 22.2/2 2 & zzzzzz! ſzzz zº
Žez /zzzz z^ Z2/. Zazz/ zz. zazzozzº &zzzzz zzzzz prºve& zzarezzºz. zzzzezzzzzzzzz zazz.” zzºzºe &-zzºzzº Zzzarºzze. - Zº cºzz/- 22 2/z-zzº e Z Jº a 22 ºz. 2% zz & Ž
..ſºrozzy &2%
-: -
Comstock's i}avis
---
zºzzzzzz zzzzzz'
Lºzzº
wº. .5%zz/ºr 2///e/Zºzzzzzzzzzz. &zºo
&/ºzzº a.º.ºzz”
º Zzzzzzzz"/4¢ &azzcze”
(222222ed. Zzz zhe Seczzozzº.
***
- - - - - - - - - - - - -
--- --- - - - --- --- -
74. ºz
.5/zzzzzzz
- *zzºz. Z%zz
*… />
2-2 -
%22 * …, 2. *…
- * : *%zzº
&zzº --
&ºr • ‘7%zz. *…... * ---
- zzzzz * -- - - - -
- - - - - */ºzze ------ aº
Zºzzº & oºzoº/ orezzouz, ſº (rear
Zaza. Zayer / &/ 2/7&z/Zºº ecºz zozzzzzzzzzzzzzzzzz z/2 z-zzzzzº Zerez . Eighte en Mile Creek
-
- Old Store House - - - *... -- º º * F.
- - - -
Lay's Tavern - º - º - º º - . - º - - º - - - -
- - - º º Tº º - - - - - - º º - --- - - º º
--- - - º ****** -- ºllº.…. º º - --- --~~~~
2?
Ozze 7222/e of Zºe Seczzazz.
ozzzzzzed. Weyozza. Zºzs Zozzzz.
--- - ‘... --- - - - > -. 7.…..... 22 & fºr ºf ze/Zºr Aeae/es, trz//, /or c//º o
- //zzz zazz & zer, º/, //, / / /?Že &^% wº 2.5%/zzºz. - Sturgeon Point -97Ž. */3, 4. 67.04%, Tº. Zes to
&//zzazzzzzar /*zz.
HORIZON TAL SCALE 10 N C H E S TO THE M ; L E. V E R T : CAL SCA LE O N E IN CH TO Loo F.E. E. T.
(G(ſ)|A 3 iſ
J) elaware ("reek
§ {{GTIſ)..N. (T)F LA K E FF}|E from me ºr D El AW/A# E D. REEK iſ [D] [D] U.N. KIF K . PLATE VI.
/Aocks of the Porzage Grouyº/
Z%e zzzzzzóez's zºzazaaze azszazz.ces Z/2 ºzz/es /rozz. A /ø/c foc/c
Calterau
ºl
gus Creek
-
- --
--~~~~~~~
White House
-
---… …º.
. .32
.5/zzazzzz
Silver Creek.
ſº a zºº
Beaver Creek
&zzzzz zzzzz Azorez 5%zz/2
-
---
7/7, -
ZZz//s of &zeez azz &/acA&
º
-
º –
CZz//s. o/” a/az-Ac S/zz/2 Szz-eazzº. - Zarzyż Wºcz/e 4-ſong a 4azoº/* -
(Z/2 ºz. zºº. 42%.
Scotts Creek K
- - *-*-
- - ºf ---
- º
- ſººlº
Sz7-2a27/2.
---------- ---
ſº
(COAST SECTION of L.A. º. ERIE from WAN. 3 Cº. 5.2 × 30.3% to CIGIAUTAU (G.U.E.
º
C
lº
E.
E.
ſº
PLATF 6 a
Van Buren Harbor.
- - - - º º -------------- ºº …
---- - --- – - -, 49 - -
Vazz & Żeac/. Little Câa adawa Creek
*-º-º: - --- - -- - --
*—s - º-º-º-º: *º- - *º- *** ***** - _º
- - - -ºº-ºº: ---- - ---
_ _ _- -
g- Ž. 27. 7… 7. s/ha/e. --- - - - - .52
Stream
---
º
º
Czz/ºr oz'.9%ar/e whºzerzea więż e/7”/arezzcezzee a/ 2/zzzzz &c. . .33 (%/ow aza' ºr covered ſº * / zzee/.
- --~~~~~-º-º-º-º-º-º:
Steeana -
House Portland Harbor
('
aºzzzzzzzzzo' ºr e 4, 5ozzo&
&reez º,
Zach º Aºnazzazz
PLATE 6 b,
Stream Stream. So Sawmill
--- - ---
--- - º __ -
ver the Cliff. Stream falling over the Cliff,
**-*-
---
AZ z//ºzz/arzzzz///zz/27. 6/
is the /zarzaz sax/z
ca/area/
Stream
- Stream & Mill
Stream .
º -
- . - - - - - -
- - º ºf - - --- - - - - - --- ---
- -- - - - - - - - --- - - - - - - - - - - - - - - - - - -
- º
- ----------------------
º º
º - - º - - º - - .
zza/r/ozze.
/a/a, waa' /…/ J'
A. Z/ J
Øeza/c/a/ º wººzzazza, Z.
zº … Z. /a/ºe.
*º- -
ºr - º º *- -->
--~~~~
- 6 -- - - - - - - - - -
w//, //zzeriºr oy’ Zow Zeac/. /////? /)azº cºhaſe.; ca. %2e
Cove landing **/~/.4%
/ºpe/edºcz/a/. c///ºr oy’ aſzyż, / greezzar/. sha/e
Stream
Stream is a
º: - -
- º º
- --- -
º - Str °anº
6.P - --> - - - - - — - - -
c//73 &/ºzzzzzz zza” &ccozzzzzzz zºº/* covereº wº, a ſºr or dºz/? - - --
Pennsylvania Line.
Zaah ºf Æzzaſzczée.
SECTION IN A N Gº. A so I toº. A glºss ºne ſºon MA Iºs Iºlº Tºlºlº II. A ſº ºf TA TRIO AND I Tºº lºſs Yº NII A ºn MINOIS COAI. It iſ lººp) P L A T E V | | |
- A LONG THE LIN E BET W E EN THE THIRD AND FO U R TH CEO LOGIGA DISTRA CTS OF NEW YORK - - - -
Aº, a dº ſº. 4 wº
- -. - - -- -- A/waz /ºrºccº and ºw ºwn… Aſºſ/, - - - --> -
, LAKE (N TARIA) Stirling. Victory. Savannah. - - Moºn eammaa. - - => → - Plaster Quarry. C ayug a B ridge - P
-- - - - - --~~~~ - - – Tse-T-T = Tie - - Fºº SN LE2^__ -
- - *__ -- gºś #º-E- - – – - - - - - - T-- - T Tºº Hº - –sº --~~~ – ºs >~~ G-> -_-_
- 4- ſ — * . - - - - - * * - - - - -- ... " - -
if E L I ºr A S M A D S T 0 . M. F. - A & M H ºf . & R O ºr A- tº 3° 0 Wº Z, 1 & 4 º, A 1, 7 & A. O. tº Aº Ağ
& cº. -
º -
- - - --
*** Ža/azzoºs º-Zºz//y /**. Area of ºne-tºne * Il-tudlow ville -
- º -
- -- - - −--- --
- - ~TS------ – - --~~ --> _s=- ---
*g p - - A. º- --~~s - - - --~~ * > → ~~~~i= e− * -ºº - E-T_- ~~~~ *
* -->== Lev anºn a *** – = − = − = −7- - - - - - - __--_ºs --~ *
−-T - - - - --~~ - -- - = sº - - --— - ~~ - - |- - - --- — - --- - - — - – - - - -
*=- - - --> - º-º-º- - = ~ * > = −e. - - - - - - - ºve-, --→ºs º-Irºſſrº |Titº ſº Tºſſ ºt, rºſºfimºr- -– - == − = − =Hºº, ſº t-
- - º - – ~~ - Tºº-T-> Fºlº-rººts_º - º Air-tº- Flº-T-ETH." "" " "I" "" iſ ſhººt- –Hº-Hº- lººr T-i-Lī- Esº-º: * Fº º *Tºtº; º ** Tºrº ======º "H" . | " * 'll 'ſ') *# "H" ſº F#EºN ºr 3
ºil-º-º- … T- - - - - - -- - Cº. - - 1 -- ºl- - -º-º: - - —tº its º - - - - - -- * - - - - - - --_- -- - L. - - - - º - - . - -- - - - - --- ---
-- . . " // 'A) /, /A/A/.5//ZAZ" º AºA'A'.S.E.A.S.A.A.T.A.' ºvers fºr
%2. 42 *7A: - - - Zºzzzzzzzzz zººard ºre s/zaze. Zºº /, /A/A's ZZZAZ rºzcceeded ºv GAAZSA Myers F.
°zzº Z, º; /* O 2.
€/ Z, &zzyazızzes of Že 5////e.
* 22, ºf . A R C E L L // S S 1. A 7 º' …+ . Aº Aº // .4 ºf / / / O Myº -
- & - ſ Z2
- *2. Žoze.
~
exº - - -
77///y timeszozze disoft/lears beneath. Fall Creek. Ithaca . & - - - - - - - -
C a _ºp eacer Mar sh. tº gº A///s Spencer. –- e = - ~ =~~~~
*/ze Zake. - º - - - - - - - - - - - --- -
- - T-T - º-> T- - is-3s T2- - º-º-º-tº-s-a-si > --→ * * ~~ - --~~ T-s-T-- ===st- > * ~~~~ — `--~ - - - -
is = e− = - * -- * * ~ * º-º-º/ > − = -- = − = * ~ * ~ * = − - F-- -
~~ T_--> — – = − = - -- - * - – - =- T T _- – - - -- - - - - - zººs - ãº- - - — - - - - - - - - -
s T = ~ -* T--> T_2 is −2−. <=E Iſ TTE Aaaa-t-ºf- – Y.T. = TIT- Vaſ–Tº-Tº-Hº-Hºº-º-º-º-HEAEI-IEIHT- ºf: - * = º-F— = − - - – FTE = −
- - - - - =&ºi=º # == ==E====== -- - = = ==== - T Ajoyº = */º sº – º - ---, º & 7. -
T.T.T.T.Z,77.… (Zeze see SZare ºzzh 36/2Zazzo 30 ft. º Aºz, Sázaza zeaz-Zºº / orzzozzzz/. Žey cºez Z/22 Zazez, Zorzez tº ºzº rozzº& 4/Zzzvºzzº Varðsſºrs azº Zerzazº: Szzzzzzzzz o.º. Zºzzage ozºzozzzzz/ &zy Shazes ºf ozºg &acewas ºxazsáozzes Jºzº Aºzcºzºes.
-- sº *zzº'szozze
º
3.
^2.
i
2 -:
F WOR7//AAS/A27% º 0° 7/4
* Cozz zazzs 22/2 /?.
ańore ſorrazzafa.
AP7////W///ZS (44 °/ F////) of Aº WWS)7,421 A//4.
- Q) r -
ºf 7/2/2//zzzzz E
i
^ºzºzzozzzzzzze
Vazzey of 7/1 razzºa.
Cree/c.
Athens Tioga Point.
-
-
-_-TTT
- --- - - -
A tºre scorzº
-- A. on .il/zzi” … tº - - zz/. Af zzzzze - 7://7tary Ž Acs *Ayaz, º, , , - - - - - - - - - - - - - - - - - - - - - - - - -- - -º-º-º-º-º-
Paſſey of Cayº Creek yº, , , , , , ºft’ ” of Aºs º /ass:Aeroºs ºs ºn ºf Zºe sº azº sº. Sazºszones , º, ø, ºs of Cºzolº Zºzeszozze of Zºe C///, / ACO (, Zº (22//* /assºg bezewº, ºe ( / / / / / 84 W 12,570 W/2. ºw
- - - - - - - -
werezzonary
-
º
valves had -
7. ///ze, Szzazzzzzz /e/Zoº zs/, /da/zz &zzº 97-are/.
Z. Secozzo, Szzzzzzzzzz), ZZzzz's/, c/ay azzº grave/.
c. CZºy ozzo. 97-aveſ with Aragºzzez’s of Z/e szz//ace”
Szoº/red roc/º indezvºzzzzy/ed. Zzz grea/ Cozz/ºzszazz.
2. (Zºy ºzzº worſ, Aragºzazzº of Zºe zoº-Z/ºe Szzazz above /ess &sºr/a///e 4///&e
2///ase &ow//voyaz &zzº, s/zzazz/ &/Zez Zºe Zzazzzzer o’ (2/ac/a/ /zzzzows.
NATURAL, SECTION EX}]]|Bll Till C, BROKEN STRATA AND ANTERMINGLED DR][FT
S/ore o/, /a/ e //ze/w//w/ (/av/azz/we (ozzº Zezz//, one /o/, ºf , /
-
-47 e. azºe 57/7/472 &/azz sºº'azºe Zºzzzzzyszze /ø///ºcſ/gºo.
Æz7& a′Z′esºzººeºezzºs /ö/ø/&cºa/, //es/nzaćove aze ºrožez &zoº/a/.
*/ A. Zhere is a zass 0/" c/a/ azza' (rayzzzezz/s o/ rock was, wer, wez, cz, Z/2 -ſ / / / /ø/ / //, // w/ e º zºo/ce/z 272 ozza' &ze /o stazzºzzº oz. 2/e eaſº/e,
s/raza, Z/2 szzz/ace /e/ow szoo//zed/ orzaz sºrzazed as Zºe/ove zzzz/zzar/ea’. or *zzzzzzzzz , º, ø, º, ø, º, ø/2 greazesz. Zºossº//e cozz/ºzszozzº -
Az z. zhere is a Zºzº mass of cay//zºº/azzº /* a/Zºe zoº sºyazazzºg &/ºrºoz.
o/zhe sºrºza a/ove, ºzo/, aſ eſ/erarºzzy sºrokº oz//ºzz// / /º/7.
* Z. Zºe sazze /*ezozºa azeº as az AC. azº ºctezza” a considerøe &ce riºd az Ze/2. Zºe Zower/zºº/ecºzy
Žass / 2.3. As a s/a/ oºzoº arºzzzzzz zaar/y Zºo ////, //e w/o/e 4/s/a/ace ozzo, as enzzzzzy Zzza/s/zzóed.
ºf 2.2% Caverzozzº &/zezzzzzy Zzzaze Öy &e acºzone of Že waves
z's seezz zear Žhe Zerzzzzzzzzzzzzz // //ze secºzozz.
PLATE VIII.
WAYNE COUNT Y. Aſastern parz
PLATE IX .
22 ºr zºo.
Wolcott Rose. Clyde, -
4, 27&azzo == −. - - - T ºnanzaga sazz (77°ozz/2. ====- *sº === == -
J Medina Szza'sſome //zzzzz &rozyz, j%. 2, ...” º ZZZzzºzzz Az/Zs of Żaze (ozzzzzy.
ºr zagazra Zºotº/22 Zºzzeczzozzº. Mºz/?” A. azeº S. /**/
SEN F.C.A COUNTY.
22.2 Senega outlet *****
- –-T - - - **** “ . . . .T. - --Lurzes
- - G = − = -O = \-As-Re E-ºn-
- T_ - - - --> -- S-23 ~ - - - Fºrenzºne-zone
-> _ --" - - - - _ --
//zozzº'aza. Sø/Z (zzozzyz. <2<2- 2…, *~22. -3%. , Aſazzzzzzzz &rozzº s
*2. *2. *zz- %22.
TOMPKINS COUNT Y.
He cror.
4, 52 r - - - - – - -
- 5%zze. — tº - Žezzzzzzzz & row/2 T--- ==== == = − = E.
= - 7ezzzz of Se/2 Zazºce 244 - – = - ET-- = == ==== == --
== ..., T- % f –2– – – = ==~~ E -— = zeved of Cayuga Zoºke
* Hazzzzzoz &zozyz, ”. “422. *see & s SAC 770% of the Z/Z-Z//ED A.I.A.A/E. J.TH-4 C-4. TOMPAC/WS C2//W"Z"Y. 27 Aºez a.d.ove Z. (272&zzºzo.
*&^22
Sº,
- ºne irrung". S.
Erin Chemung Sº
CHEM UNG COUNT Y. Newtown creek --Redºn-Creek --- wn — ``
ſever aº – - -- § JAlluria. Bottom º –
N**** => − Zºzzº - — T
Havana. –T- °rey Shades-zz Szyzz/stories . .
T- --
- –- T-- ºzzº
Prº - - -------- - - = - -
//e3% Sezzz Zazee ºfficiaº - -
7;º-T cº-ºr- - T - - - -
== *** * Z.Z. 57.22; …, 27… Zzzy Szzzszzes. T-
- T- “. - -
ºz ºnes azºº Szºszzes
-
--
-
7,727. (ºrozzyz . Ž ^^ - or w a g - - o zº o zz, zº
WAYNE COUNTY Western/ear’
Ontario Walwor"
ºzzº
1 - 4% º' azzzzzzzzza/*2
437 A.
enesee 34.2%; -
% %.7%y/*
fººtaz Zimestoſzé.
Aſamzz/Zoz &rou/*
C anandaigua.
Mangye Ster. —= -> -
Milo . Tº arring"
“ — Toºn -
1 levez of Grooke” - zºng &row”
Żyż ż - - - - ºf --------- -
ONT ARVO & YATES COUNTY
B, enton.
‘sl
= —Aarzage 6 row/2
s
-
–
-
=
-
-Gerzęsee 34%
7%zZZy Zizzesłozze
Azerzzzzzz Zimeszone
J’
Troupsburg.
=0ºd Red Sana'stone.
Sarza’szones.
-
-------
STEUBEN county -
_- –-
_- 0Zzve - arº z 2,…, - - -
---- = ~....…. ------ -------. . . . . .” ::::::::::: **** ... *.*.*.*. * **: **
Ba
th
–-Tº-T --- -----------
- T-TT Shales area.
--- -
8
º
9.
º, Greenish arº grey Sazzstone - - -
_- - - - . ---
- –––.---z-z::::::2, 72, _______------------------ ____----------------- ----------- ______------------------ __...------------------ ... ------------------ ---- --------- -
_______...-------------. ...--------….. =- Izzº Zāº ????--------------------T .…-----------~~~~ ... I ----------~~~ ---------------T"
…I…----~~~~ ------------jºº ºf Zºe AErie 34°
- - - - -
- - Scottsvill PLATE XI.
P. ochester MONROE COUNTY . W . - . . . . T C 0 tisville
2 * 5 ºut – " - " -> ****
- - __ - . -- - - = - - - - – - T- – - -
/. Øzzazzzo. 4. - - - - - - - - - - - - - - - - - - - - - - -_ - - (2/20/ Z ar Sazz (ºrouſ”.
*…, º Shºw/e Zimzes Zone 5
..!/ e º z // & S or /z & S / o yz e. ”2 /ø. (ºroz/z.
LIVINGSTON COUNTY . -
- York. Mount Morris
Caledonia - – º – - Moscow . º
: Aorzaze Sazószozzes & Shazes.
tº ºozzezzz S/a/ect AZazzsºozes.
--------- ---
(as/…/ºza. shaze.
*- - - (7.277 esee 5//w/e .
- Peace of y'arety ºf restone.
ºzz A.
- - avey-ºº -z: - - *zo,…... ~42s.
07.07, d'aga. Sø// & Zºo Zzyzº’. 2- º, Z//zzzzz/Zozº (; 7.0///z *zzzzzz.”
| -
ALLEGH ANY COUNTY ***
ſong", ºne - -
s - sº
Wells ville = === == º º -
ſ: d zz/ted. Sarza’søzze.
La Ilie & Cº. ca. . --~~~~ -º-º-º-º:
*… • ** - - Cold Creek. - Genesee River
ºzs Sz - W - º-
27. 'ººzzzz & *** "X - – ºr -
Zzºa &zz, so 2. % zzzºz. --- -**- *"…,' * -->
*** ******::::…:
Poi t ozze.
"tºº -
" " "tºº
---------------- -
***********------------,-,-,-,--
- º -- cz/. - ------ -----------. Tº ... . . . . . .
*** ***… s.….8, --,-,--
- - * - - - ---------------------- -----------
- 3.
Merez of /a/ce (ºnzazz-zo
*… Barre
.S.
- - - —aſi-
O RLE ANS COUNT Y. Gaines. – “H ºr
ºraza &zºozzy.
A 9/72 arzo - - - --> - -
CZzzzzo” (ºrozzzz-
s
GENESEE COUNTY
-
Creek.
&zº,... º -- -
*azzº. ººzzº
6.5-2. //a. - 77- /ºro tº- - -
- azuzzo” (” -
*zzzzzzzzzº jºs 5%zze.
2×ozcz. -
//zze, z *… --
zºº’eszo
- - - -
---------------
T- -- ----------------- -- - - --- º
7, 27,º, ZººZ *
Zerez of Zaz-e (2222ario
-
- - - - - - - - - º
River.
Alleghany
---
- - - - -
- - - - -
--------, --
----------- Zerezº Croo/ceº/a^e zºº
---. Zerez of Zaz-e Aºze º
-----------------------------------------------------------------
Zºzº, 2/ Zazzº ºzzzzzz zo
- º
334 -
Lockport Pendleton. PLATE XII .
N A G A R A CO U N T Y.
Ørozzagasazz ºrouzzº
Zizzeszone 2 47.
s } of the cºagara &rozyz.
Cºzzzozz grozzz.
A 27-2arzo.
s
º
Tle
E
R
E.
C
-O
U
N
T
Y.
ls- - - -
- - - º- ºr erºesee 5.'raze
- - - - - - - - - - __ Place of the 7'ºzzy
- - - - - A'ncrºnzzaz / Ernestorte
-
- Leve/ of Lake ºnlario.
sº
^2. - - ZZ c. - - - - -
dº a ſy & - *Zzzeszcze * Zºe...” zzeszo. 77 a 7” * * * * G 7- o zz za .
CHA UTAU QUE C O U N T Y
zºad ºr
Stockb
_**sadegalºke- stock”n - _** 2%zeraze
- l
- - rang!
- - = ** ~ * –
–º - - - - - - - - - - - - - – “H - - I’an atmla - -
Fºº . . . . . . . . . . . . . . . . . . . … Tº zoº ---T : … -------------- Tº " ºf -
2 azzaz &/ozcº S.
- &reezz, Ozzº
-º-º-º-, -º-º-º- ::4 12-foss º º - -- ~~
s
s
s – /or age ºzozyz. ---
* --- -------- - - - ------- - - ----- --------------------- ------------------------------------ - - - - - - - - - - - - - - -------------------------------------------------------- "ZººZºº...T.Z.Tº "
Zziº Zºº. 33% 7"
Zerez of Zaºke (2ndarzo Tº
Summº
**a**
– - S’ wºu
- - - Szzzzzzzz
3
s
ºf 3A'
s
Swim maz
wºº F.
*34.
& A.
|
\*,āş,º,
*
:
s
-
i
i
§
i
SAC 770//rom ſhe head of C4X//04-/A/C/a/ /7//ACA & Zºe (2///ZSZZ A/VA/2 az AM/////C4 ar//zzzzz zhe 2/evazzozs adove ZAAA' (2WZAR/0.
Zerez of Zajce ºnza, a 23r weez ºoº-e zºe jaze-
7"-a.e. water-e-ey
Szzzzzzzzzz.
zazz A'
y
73
5
A.
§-
\
s
i
S’ - S' wº
wrºzzzz!" r2
ºrzº º
/
- – T- º
i
s
y
2^
-
;
/s
-
-
\ſi
ſ
---
ſ
*
* - / erez of Zake ºrie ---------
S/C//0/V/oz, &e 6/...//5//, /t/V//ſ aſ .4%////.4 zo Z.4/CAE-Z//Z' a' PO/7ZAWZ, ZAF BoA ar/zzºzzy Że e/evazzozs azove Z. 4 ACA 04"7:4A ſo
Zerez of Zaºce (2ntzarzo. 237 AE' ºore 7zze //areer
----------------------------------- ----------------------------------------------------------------- ---------------------------------------------------------------------------------------------------
ºr ºve.’
I, FRIE -
NATURAL SECTION ºzy z/22 G E N E S E E R V ER /-op, MOUNT MORRIS zº, PORTAGE
N. F.
Mount Morris ~
-- P- -
= ~s --→ Tº s = * =~~~~~~zº- --- - - -T ===TE==T--> - =>==sº- =>S. = ~s - - -- ºf ==> =__*s ãºs. s T-
*—- sº — `, ſº – ºf Tºg *"... I 1. F- ~ --> = ~~~~~s. =_5= Sº I - > =4– ‘S- ºrs sº - sº 22- - -- - S- —- – sº-
- ſº. T \s - *------. - - Eºº- –- Tº ºr - - Xī’ſ - __ sº-, … Tº - º: - - rvº H== --~~~~ -º-, - - -- - - - º – ETº -- - - - - –
===============s==========<=4===&s * = −ºsº-ºººº…tºs-ºs---> A ºfflººr- - ºf 2. - ºyºº.2/7 T *r--- " ſº- T Sea A_s====ºgºs::==== Yºº-sº
-- -- - -------- --~~~~~~~~~~ -- - --- -- -x->-> >~~~~~ - - -- E- - -> -º-º-º- - --~~~~~ --~~~~~~~~~~~ rº- - --- - - - - - - - - - - - - - -
.S. 72 ºz Z 2 .5-
Tº a z. z7 a z. zz, A Z & Z & Z o z. z º.
&ezzese, s/zze Jezruction of (fezzerea .9/zzze & 6%r/ºwa. .5/#axze
Z2 /2 / 7' 4 & // /2 /2 2 ZZ Z-2
NATURAL SECTION aſozzº, Z/2 GATTA RAUGUS CR E E K /º/, LAKE E R E Zo zºne Zzz/2, above LOD
WA".
Złoczew or Z/2 /ø//zze ºzºo/,
- .4//zzºzz/ //z//,
Alluvia/ Terraces Rocky Cliff. of Pºrtze 6-24%. wº. A/Zuzazzzzz //z/Z, ºr z/e 4, 24. Zºo” 2/// e/e7%
- - - 1770/€/// --- *
…
- -> T- _- –77-72 I-I-T- - - - - rº-Cº
_----->~~ - T- ----- T- Cº- --~~~~ - --- º - º
- - - - –- - T- - - fººr). - ºxº~~~ - rº-º-º-º-º: zºº 2 - "Tº - -
= - — — `--- 4…º & rººf ººº-º-º-º-ººººººº --~~~~
>
A, a dºz
Vertrait, on
youth barek of Gºzº. -
SECTION across the FOR MATIONS he/weezzº C L E V E LAND or LA K E E R i.E 3 //, M S S I SS J P P : R V E Fº
2,222// / /* Ávaſ/zzº
º º "EZ Dº tº 2; -º-º-º-Q
- - ºx-º-º: º º
Ø º ſº.ſ.º. ºf K rº. Yº
ºğ. *º º §º.§ { º 3. ſº º
- — `Sºº- r & -.
PLATF X | | | |
*A*-
Portage Lower Fall
Fartage
Middle Fail
ºf
*::::A;
%xº~ JazzFeone
CZzzº j.jø /…/eſzewºſzczz/ºr
.
zzz/ *//ocs zzzzz/ /ø/zyż A//wwwaz //t/Z of
-
-
- ºr r-
—
:
:= -
-- -> *-
- > º
= º: 2.
: - - - —º C#, cinnati **
- 7' At 2 (7 ºr - - - - - - -
º e ºf f / / 7 * * - - -, * -- - - - - - - -
º - - f : * o ż ºr "o c. 2 # / e / 2 meraſ” I, ZººZºº # / / / / /* I,7722 & Z & rºle, C 7 º' Zºzº /, frºm e º ż ozz e + , , , . ~ -
> - º - cargº (arºorºº - -T te:- ( / ‘’’ s - is Cºurthus -
*. 5–- - - - N --~ T. > T- - - - =- - 2 ºzzº – – - - - - T - - – tº *= :
- T T – -- - -T— - - T-z. º - - ------- –7 //º/, "cºcº //re Zazzarazza º yº /a/ / – V_ - J_
- - - –" - - - ** – T Cºezzzzz --Tº. L. : - - - - - - T--— T- - --
--~~~~ Ozzº - T- *... ERIE
--> --
S.W. Carbonirºu, or at Mºrizºpf Zºznº — -
/ / / / ºr .5/ a tº a ra z/ //z, z/., o zz /; , , , ,-
s
t;
9?
º
S E C T O N acroºr //, S T A T E of N E W YORK fºozy, Ł- A K E C H A M P L A N of the N. E. ſo LA K E E R i E on the S. W.
ºfer of sºccess zoz ozong Zºe &//ezºezzz zºo.c4-3 ºzzº (ºrozzy, 5.
Shewing Zºe
ſong/om crate
#
#
y’
White Face Mountain.
5,300 2-2 ºzºv*e 7zz, sºazº.
--- -
- - - Gro º _- –º - - E
- _- — –– T ºº:: *** 3-
- - - - - - - - - - - - - - - - - - - - - - - - - - - - - -
- - _------—- - Artant s
--- _- - - - ->- - - fºrt - - -*.
--- – E- - Zºzzsº dºoz. - - - –- Grey & 3.141* ºt, " *...
- - - * – - --- _Grº _ _- - - tº, at “ ºt - :
-- He/gºž Øzzºtzºa. º zº - Žºrž ºzzº - –- - Lºſiº is.” 1ſt __^ *-2 -
- —- - - -- -T -- - ^^*— - - __--→ ..., , , irºz ------ - -- - --- - *... ~
— = − __ – T –- _- = zºoz Azzºz º.º. ===zºz -—ſ - 7° ºf 34 A R Y, ºr HYPO (AENE SYSTEM STS, T
-- __ –- - __- - - - - __ º- T ºr, ºr º_- -
ºr - - 7 ºr . 7 - - - - - I - - - º' -- - - * - - - - -- - - - - -
/*e interra/ 3&reez, Zºe S. * *cºrezzº ºf this secºzo” arº &e cozzzzezºezzº of Že one ºzovº º 'ººzzº is occº.zzº cºzzezy Ży roºs º ºr ººze ºrozzy,
*
E.
- - - - - - - - - - - - - -
º
º,
º
º
Linh. of Enoco Tr New Yºo Rº,
_- .
|-
|- ºſſ H.A.TXT GRŪTINĀTĀ TIIT NÆGTØRTXO^T* ŞTĀVĒTĀ Ģ Ī ĶĪ JĀTĪGĀTĀ KĻĶĪTĀ.
-
|
^ °^ TILVTI
º
º
º
-
AZrs. .S. Aizzz.
-
PLATE XVIII.
Ząż, o/'Anazcº.
II, ODI IFAILILS GENESIGE COUNTY N.Y.
-
*
-
-
* * - - .
- - - . . . * - - -
T * * * * * *** -----------------. -
THE UNIVERSITY OF MICHIGAN
—S .
DATE DUE
:
|
NOV 1 o 1990 - ,
i
|
|
i . . .
-
{
f i
| i
!
- |
|
i
; -
| {
ſ :
f º
| .
| !
: DD NOT REMOVE
| -
!
. . . . . | MUTILATE CARD
s: # *.
. . . . ºº: "...º.º.
w a ... 3 * * * & *
- tº ſº." ºs. §§§:
sº tº º-sº * ... * * * * * * * * *
ſº . º - º º * * *.*.*.*. * * *... . . wº :
a. º:::::::: • * . . . * * * -
g E. º sº
tº
a * º
* -
*
; : * **
º ºg
lººkºº, ºws
ºwº ºº::s
* * * *s & ºf sº-: a sº
ºº:
º
* > . . º
º ºg
***º
º:
Ǻ * * *
º ****
º
* = &º º,
&: ; wº *º
***
e º a 5.
- * * * *
* *
º
* * * *
º *...* * * * ...
§ºre ºr a . . . . . .
º'º - ...","."
* * *
* * Fº
sº ºf 3
º º
ºlº. *** **s, *
tº sº.
º sº. sº
ºº:
*ºr
tº cº-
* * * *
º:
sº
º ſº º
*** * * º
tºº, ºf .
º º
º.
º
º
º
º -
º º
º:
º
׺ sº:
sº º
º º
- º
§º º
º; gº sº º
º º fº §:
j § º o
º lºº.
º d
º
º
º
sº º º
sº *ºº
º
sº º -
º
Nº º ºsº -
º' ºw º: - wº
ºº:: * * * * Fº
ºlº Cº.; º
º º º sº º: *
sº ºr º
* * º: º:
º ºt º,
º Sººº. º sº
* * Nº tº -
º Cº.
º
**º
º:
w º:
º Rºsº
sº tº -
****
º ºgº º :*
Xº º:
* g. sº
* * Rº:
d *º.
º
º º -
º º
sº
º: ~
º
º
º
sº
- sºlº
- º:§
º
º
º º
º &
ºº::
º º
isºtº º
º tºº.
º
ºgy
sº
º: º lºº
Kºº. º
Ǻº *: º
º ::::::::::::::::: º º
sº wº. º:
º º
sº sº.s º
- Rººg.
tº gº sº
tº: C *º
ºº º
º: Fº
º
§:
ſº
- º
§
sº º Nº. º §:
º kº &:sº º
Fº
*:::::::::::::::::: *º
§º º º:
ſº
º
- º
sº
º º
* .
ºº:: º sº
§º *:
**** º: ** --->
- sº
º
§
gº
ºº::1
º +
###########
º º: § §
§::::::::::::::
Sºft º tºº. º:§ -
º º flºº - -
ºº: sº sº º sº tº:
º º º - sº ºś
sº :S sº º º º º º Sºº !
*º § º sº º º
º É
º gºº::
§: º
- ::::::::::
- 3.
º: º ;
º tº:†: º 4
º §: º §§ º:º; ſº : s t;
sº º º ſº ::::::::::::::::
º *} º
ſº. º
º º: -
~ §:
§
::::::::::::::
§ º *º w
:::::::::::::::::: sº Nº rººf:
º º º
ºf ºs º º:
§ º
sº º
º
sº
sº *&ng 3.
sº **
sº
ſº *
sº º:
sº
º zº
º sº
rºº ºº: ;º. *†
Sººº. ºr sº sº
sº Hºw
§º:
&
ºirº
::::::
%
-#3.
sº
sº º
rººt
º
º
?? º
&
º
ſº: º
º *.*.*.* º -
º *º
º º º
º º
º º
º: *º
sº
º %2 gº
º: º
rºº & &
sº º
º
º
º, ºr Hº:
§:
º ****
Ç º º --
tºº
º
\º º
º