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oem _ 8 ean ‘ a - oe Tg pete t cow ert @ ree. a cheiels ¥ see Sar ee A wm pm nhs ae so ERM
eel in shee ane = = = oi a — . a a ne ox = ea tar - ate eels a - re ee en Ae ere
nse ae mm i a ° . x *
——— - a ts - ad : . pteern <=-weere 6° ee “Se —- ee -«@ nae oe orTe wane eee ee ~~
7 - a ~—— a ie ma _—— <= rie + bd — - . a alt di ana
EME es en late ae om - an t= * ae te tk a ee ce annie LN - we _ 7 °¢ Soe were * -
a ewe een eS eee . - - SY Seaeweees “See SSS vote = * = less «eee @ ee, c wata w eeaet § 2m PSS
to? Gage 0 © Stew eet fee | - me »o- 7 “ meee 2 eer fies 7 ~ —sP - ee rk aed) Se eS OSS oe © a es ea
= . a = aoeeea « gh, — - a - 7 7 ae we ee «<= arn - - » she oe 7 4 ° - ° 7 aw ower o, ower oe te at emene oe i eo 1. tae ohrte gee wre ree --
- te —— - _~in «= o 2 ° we wee een — = ee aint a
er ee ease illite at — a * a ot mares ~ * * ‘ = - Cee ee se eX Sk pee ann = poet tue o «* ~_< sew ew oer — oe se nr ="
_— t= oun Ce 6 - Sinha ne ee een “4 : : a - — ba a - ee : mel av ee ee a: gm tae . het ee ere oo few —*« lm Sig eee Migr ee 7 ee
- ad ~~ Sk ee al a 7 7 - - : = a —— * wesw * \- at cinaten arene oo UT ew —_—* amas te © 9 Mere 2. oe Oe ewe ore
. _— - ie =“ eit ere he ~~ es a! a
‘5 ~ mes 7 oe —— f : : . aT pee —* Ee sh ree <5 ome = ‘ * ‘ ed
a at ae ue i o- - See ne S a. ce hes © ale Mee ee eee
Sanderhing, “Galidris eu co'phia'eas \ Pallas)i 30a). 2 eset.
Marbled: sodwit, —E iim osa edie Chinnaeus)ians4.. 4 eee eee
'Hudsonian godwit, hbimosa., i we mids t ean ( biandeus ae. ee
Greater yellowlegs, Totanus melanoleucus (Gmelin)....
Hudsonia’ curlew, Numenins ‘hudsoniceus Latham: >-:>.-.-
Bobwhite, Colinas #1 eaten adit se leingeeis eee ee
Marsh hawk, Circus: huds om dats (Comeacus) eee ane
REPORT OF THE DIRECTOR IQI4
Coopem haw sy ecctpirer cooperi (Bonaparte). .<.6:ietke.s-
Castanieeecmivineat 2 Gam tls: <(Wailsom)riss5 on ee ee ben ee ns
Red-tailed hawk. Bu Pew borealis: (Gmelin)... .scccideee cs
Swainsonusbaywis BDuted).swains.onl ‘Bonapartée.c.......0..<%.
Greecmyawh scotia ptex. n.é-b wl osa-(Porster) 24.04.45 --
Baw cewewoe td ha oi lula -capar oc he (Muller). ese
Burrowing owl, Speotyto cunicularia hypogaea (Bona-
PESTLE Se CRA" scar ORR re reach vse ean a Wena eal ty 5 Sake athe Ps
Black-billed cuckoo, Coccyzus erythrophthalmus (Wil-
SUEUR ERT TAA thas ots acape take, diets ware. o Pepseeen ata sean SG alo vieteye alee arn ae
Chaneanshers Cery le) al.ey on /)(Linhacus,) sacs istic cco eteenes oe.
Hairy woodpecker, Dryobates villosus (Linnaeus)........
Red-headed woodpecker, Melanerpes erythrocephalus
COURS ret ot PS eet ee GARE ea oe Pe is ean BS oS bahia
Red-bellied woodpecker, Centurus carolinus (Linnaeus)...
Nicht. hawle: C hor deile si ivr ec tata ws. (Gmelin) 6.70.
Chimney switt, Ch aetine a sp.edliag te ar (Lintaeus)\.. da. hues. 2
Moinebird,. hy t's wil ws byes diy tls. Cleiamaeus) cabo... cues. 3 ae
MAtRAnGAS kine bind, aL wy fai mrs. Wy Cplet dl Ciel WS. BOD Wie ss bop fase e sts
Fored lark, Otoe.or Sal pes tr 2 Ss CLinmaeis))”. . 2 celeste fase
Macpipe-P.c apt Ca (heutd stom darn C Sabine) cc 2 od. eerie oo
Bobolink, Dolichonyx oryzivorus (Linnaeus)............
Ss = = SS HS
Yellow-headed blackbird, Xanthocephalus xanthoceph-
aoe ota parte)) si. ee per ee a tea a a UN
Red-winged blackbird, Agelaius phoeniceus (Linnaeus)...
battimore oriole) lect erus: pal bala Ceanitieus)s 2 4 ee ee
Butlock oriole, heterus bullock (Gwaimsot) on... 2.3. “Aico.
Rusty blackbird, Baphacus carolinus G\yuller)....- eer
Bronzed grackle, Quiscalus quiscula aeneus Ridgway..
Evening grosbeak, Hesperiphona vespertina (Cooper).
Pine srospeak, Pinicola enueclbeateruke mc ira, CMiuiler):
Pumplestinch, (Carp .o-d acs: -purput ews. (Gimelin).. .422052-
American crossbill, Loxia curvirostra minor (Brehm) -.
White-winged crossbill Loxia leucoptera Gmelin...........
Hoary redpoll, Acanthis hornemanni exilipes (Coues).
hedjoliear Gants: bin aria: Chinnaews eae. aah oe © ee
Goldfinch, Astragalinus tristis (Linnaeus)..............
Siow. biniuse, Pfectrophenax nivalise@Einnaens)<..). on.
Hapland lonespur, Calcarius lapponic us) (linnaeus).>25).
Savannah sparrow, Passerculus sandwichensis sav-
PREM IAEA RM VLINLSUEN ots c\t Nake 5 wie 'e ain sana oicavern era te ac HAA OE
Leconte sparrow, Passerherbulus lecontei Audubon....
Lan. spirrom, hommestes gramimacits (Say )ivo 2s.
White-throated sparrow, Zonotrichia albicollis (Gmelin).
Swamp sparrow, Melospiza georgiana (Latham)..........
Cardinal grosbeak, Cardinalis cardinalis (Linnaeus)....
Bine erosbeak (Guiraca caerulea (Linnaeus), 5.0... e:
Indigo bunting, Passerina cyanea (Linnaeus)..............
Lark buntme, Calamospiza melanocorys . Stejmegers:-.
Louisiana tanaser, Piranea ludovirttrmra CWilsonycsse:. ..
Barn swallow,-Hirundolerytirogastra’ Boddaert...c...2..
:
|
II4 NEW YORK STATE MUSEUM
Bohemian waxwing, Bombycilla garrula (Linnaeus)......
Cedar waxwing, Bombycilla cedrorum Vieillot
Warbling: vireo, Vireos gly aes ive Victor)... sen a ae
Black and white warbler, Mniotilta varia (Linnaeus)........
Tennessee warbler, Vermivora peregrina (Wilson)
Cape May warbler, Dendroica tigrina (Gmelin)
Yellow *warbler, "Den dr otc -ares biwa “(Gmelin anes > sa. eeee
Magnolia warbler, Dendroica magnolia (Wilson).........
Bay-breasted warbler, Dendroica castanea (Wilson)
Blackburnian: warbler, Dendroica fusca -((Miiller)..........
Water thrush, Serurus nov e bor ace ais 59 Gmelm) -ee_e.
Wilson warbler \W uliso nts *pmws?1lta “CWalsonpee ee eee eee
Redstart, "Sievop hac a raat toma“ hinnaens)\ sate eee
Catbhird, Din mie te La scat othamle ns 16) (Ceimmaeis)e eee eee
House wren, Troe lodiytes aedon “CVienlotyeor... 2 eee
Short-billed marsh wren, Cistothorus stellaris (Naumann)
Long-billed marsh wren, Telmatodytes palustris (Wilson)
Golden-crowned kinglet, Regulus satrapa _ Lichtenstein.....
Ruby-crowned kinglet, Regulus calendula (Linnaeus)......
Olive-backed thrush, Hylocichla ustulata swainsoni
ov love “e) 6 in te mae
oe ee eee eww ee
(Erschiind i tye 20s iS eee oe eis Sener Rca CREE IG Ine fo)
Robin, PA anes t Le 1S) lit S mat OM ats leinncens) an pee ete
Varied thrush, isco re a si aaie varias) ( Gane lign)y ae re eee
Bluebird’ --Si.ad wa eri a lors, NG immaetis) sto. ee oe ree eee
Marsters, C. E. Albany
Rutted ‘grouse, Bomniasa wm bell us. Chinnaeus). 22a
Amphibians (casts)
Franklin, Dwight. New York City
Spotted salamander, Ambystoma punctatum (Linnaeus)..
‘icetssalamander A mbystomartig ran m) Greena yea.
Red salamander. Spelenrpes:rdbes «Datrdin) \.-iierec veers
Spade-foot» toad) s“Scaphiopus ‘hol bwoo ki, (Eagan). 2...
Spring ‘peeper, “Hyd a ype kiemin £1 SStorehes tee eae ees
eopard frog, ead 1a fp pie nis) Schreber : ess i meee easier ar
Pickereltirog ka ta. pia lie t nis averConte. ey ens ole ure =
Green iror. Ria nal je lanmiaytar Wandin a. or «cepa ee sists «pho here
Bully frogs Riamiat ‘cakes bien ana. OS Nave era). atte). ee Serres
Wood wiroc. Ika nats yl watinitea, em@ente i kvnvery =>. ge pete
KH Hew NY HN HY HD 4 YD HH BSB HB RR eS
KH HN WwW
SS Se SH Se SS SF SS SS SS A
CONCEPTIONS REGARDING THE AMERICAN DEVONIC!
BY JOHN M. CLARKE
This theme has seemed to me appropriate to the present occasion
because, primarily, of Professor Kayser’s positive influence upon
the accepted interpretation of the Devonic system in the Western
Hemisphere and, in a broader sense, for his long and intimate con-
cern with the various aspects of this great period in the history
of the earth.
It is thirty-six years since the publication of Kayser’s important
treatise on the Lowest Devonic Formations of the Hartz Mountains,
and this, more than any other single work, inaugurated a recon-
struction of ideas concerning the scope of the Devonic system; in
so doing, it created new problems and inspired investigations into
a wider field. Thirty-six years ago the writer of this paper, truly
a native of the Devonic, was fresh from college and full of en-
thusiasm over the study of this formation. Throughout the stretch
of years since then, both have labored continuously over the
Devonic problems, for much of the time in close and sympathetic
touch, the younger man receiving from the elder, in information,
suggestion and inspiration, debts which can be repaid only in service
to a common science.
The State of New York, which has been the writer’s port of
departure into this field, is very properly designated a Devonic
state, for more than one-half its area is covered by the rocks of
the period, and the succession of its members from base to summit
comprises a record whose pages are almost intact and effectively
illustrate the variant happenings of the time. In America we were
long in the way of endeavoring to square all the Paleozoic forma-
tions of the country with the New York standard column. The
work of the founders of the ‘“‘ New York Series of Formations ”
in establishing their classification, nearly seventy-five years ago,
was well done, but the amplification of our knowledge has now
clearly shown that in all elements of the Paleozoic except the Devonic
(the Cambric, Lower and Upper Siluric and Carbonic), the New
1The distinguished career in geological science of Professor Emanuel
Kayser of Marburg was to have been specially celebrated on his seventieth
birthday, 1915, ‘by the publication of a Festschrift of essays by his
colleagues and students. For this purpose and occasion the essay here given
was prepared.
116 NEW YORK STATE MUSEUM
York record is imperfect, both in sedimentation and in life; not
from extensive erosive destruction, but from minor diastrophies
and unfavorable geography. But the same growth of knowledge
has fortified the standard New York Devonic section as thoroughly
complete and indicial, lacking in no essential detail in quality of
development, presenting in some degree at least all the phases of
the system as exhibited in its transcontinental development, how-
ever these phases may vary in magnitude from great to small.
It is within reason and accuracy, then, to say that not in Devon-
shire nor in the Rhineland, not in the Urals nor in Siberia, not
on the Bosporus or in South Africa, not in the basin of the Amazon,
of the La Plata or in the Andean Cordilleras, is the full and
variant succession of Devonic events so well recorded or at least
so clearly and simply presented, and perhaps so fully known, as
in New York. Upon this stage the successive scenes of the great
drama were set without serious intermission and the players made
their exits and their entrances till the curtain fell.
The panorama of development in Devonic geography and life
here set forth has justified the arduous years of labor spent upon
its elucidation. The efforts made to turn upon the New York record
every ray of light that any other part of the earth could contribute
have served to establish its integrity and to fortify it as the ideal
monument of Devonic history; while, in its turn, it has responded
like a Rosetta Stone, in helping to decipher the significance of the
fragmentary and less known. Its problems are as many as the grow-
ing host of students which later years have drawn to their solution,
but there are some of general import bearing broadly upon the
interpretation of the system as a whole to which it is here designed
to make special allusion.
I THE LOWER BOUNDARY
The limestone faunas. The problem of the base of the system
never became a matter of serious question until brought into the
foreground by Professor Kayser’s proposition that the limestone
faunas of the northern Hartz and the F, G, H stages of Bohemia,
which had passed as Upper Siluric, were logically and more ap-
propriately to be regarded as a deeper water facies of the early
Devonic seas. In presenting the broader correlations which resulted
from his discussion of the general theme, Kayser included with the
equivalents of these misinterpreted lower Devonic lime faunas,
the “ Lower Helderberg” formation of New York and its various
subdivisions. Just here was the entering wedge for the American
problem. Soon Tschernyschew in the Urals, Barrois in the Asturias
REPORT OF THE DIRECTOR IQI4 II7
and northern France, added confirmatory evidence for the new in-
terpretation, but still Kayser’s correlation for the “ Lower Helder-
berg”? of New York remained obviously based on literature only.
In those days an intimation of this kind coming from Germany to
America, for the time being was lost. Under the best of conditions
it takes years for the suggestion of a foreign literature to percolate
into the counsels of the coworker in a different language. In 1878
and those years, few American geologists of influence knew any-
thing about the German language or of German geology, and
Kayser’s suggestions, so far as New York was concerned, fell on
dull ears. Ten years passed before the evidence of the Devonic age
of the Helderberg formation was summarized in detail and set
forth in a New York publication, and even then it was presented in
tentative form. The writer was responsible for this presentation.
His chief in the geological service of New York, the distinguished
_ James Hall, was so absolutely hostile to the suggested interpretation
that, in order to even secure publication for this array of evidence,
it became necessary to change a positive argument into a neutral
statement of facts and all conclusions into queries. But for New
York and America the “ Hercyn-frage” became the “ Helderberg
question,” thenceforth quietly but effectively argued with intensive
massing of the facts, in which a strong part was taken by Schuchert,
until in 1908, twenty years after the effective proposition was made,
the Helderberg formation with the profuse lime-faunas of all its
subdivisions save that at the base, was formally incorporated into
the Devonic, in a revision of the New York classification by Mr
Schuchert and the writer; and there it seems likely to remain.
The embarrassments which involved the acceptance of this ap-
parently simple proposition were, in actual structure and fact, more
weighty in effect than was the widespread and outspoken antagonism
in Europe to Kayser’s proposition. Here there were few parties
of interest and here the succession from the Siluric upward was
unbroken, either by erosion or disconformity.
In both-countries the abstraction of the Helderberg equivalents
meant a paring down of the Murchisonian conception of the Siluric,
which, through Murchison’s personal intervention, had been deeply
engrafted on Hall’s construction of the Siluric here. This procedure
was of serious import, and a consequence has been, for New York
anyway, a reduction of the Siluric (Upper Siluric) to its lowest
terms, that is to say, practically a reduction to its Wenlock equiva-
lent (Niagaran), supplemented below by heavy local sands, and
above by local developments due to the peculiar geography which
118 NEW YORK STATE MUSEUM
made and unmade the Salina sea. The particular aspect of the
problem regarding the base of the Devonic that we are now con-
sidering has a somewhat localized significance in America, for the
lime sediments of this time, with their rich faunas, are quite es-
sentially (though not exclusively) of Appalachian origin. Through-
out the great stretch of the Appalachians from southwest to north-
_ east, the Helderberg seems only very gradually to become disen-
tangled from its Siluric.affiliations. In the State of Maryland a
great mass of lime-clay sedimentation (Keyser member) lies at
the base of the Helderberg members as developed in New York.
There it embraces the maximum sedimentation of the lime seas
stage and its fossils have but partly disentangled themselves from
Siluric connections. In New York the place of this formation is
held by lime units which fail to carry the Helderberg fauna and are
therefore excluded from that formation. In Gaspé bay, on the
other hand, in the far northeast Appalachians of lower Quebec
.(and probably in the extensively altered regions between New York
and there), the discordance between the Helderberg and the
Siluric is absolute, profound and fundamental. There the Siluric
failed entirely or has been ground out by overthrust. Farther
south in Gaspé, conformity is resumed in strata standing at extreme
angles, but here, at Percé and in the head of the Bay Chaleur at
Dalhousie, the aspect of the correlative lime sediments changes, and
in places a large element of Atlantic species is introduced into
the fauna and we are no longer dealing with like quantities.
The sandstone transgression. It is well understood that the
shallow water transgression of the early Devonic was vast in its
amplitude. At no level in the Paleozoic column is the overriding
of the former shore lines by the shallow marine waters so emphatic-
ally marked. This extraordinary transgression resulting from a
slight but almost universal negative diastrophy, spread over the
earth a fauna of large proportions and homogeneous character, in
great part a derivative from the deeper lime sediments of the con-
temporaneous sea, but always an adjunct of the spreading shallow
waters. As the transgression proceeded, it carried with it species
out of their normal development basins into others where they never
became climacteric or elemental, but stand today as a key to the fact
and the direction of their migration. It has been thought that with
the close of the Siluric the great Arctic bay which reached down
into the interior of the continent had become largely obliterated,
but this contraction seems to have been essentially at the south and
the northward and westward transgression over the north Atlantic
REPORT OF THE DIRECTOR IQI4 I1G
lands of Laurentia from the bays of southern England, Belgium
and the Rhine brought into the embayments of the eastern Ap-
palachian rias, in Maine, in Nova Scotia and New Brunswick,
percentages of Coblentzian species quite foreign to the sandstone
or Oriskany fauna as it was normally developed in our interior sea.
The presence of these Coblentzian species in Atlantic lands is itself
another confirmatory evidence of the upstanding and overridden
land bridge across the north Atlantic continuing onward from early
Cambric time into the final and continental phases of Devonic sedi-
mentation.
In Appalachia, the spread of the sands was not alone shoreward
over the low-lying rocks of the Siluric, but the disastrophy must
have been the slight movement of a low, inclined plane whose nega-
tive motion in the old land was counterbalanced by a positive move-
ment in the region of deeper water, for the earliest Oriskany sands
are notably calcareous in the fields which had been occupied by the
Helderberg sea, but as notably lime-free over regions of the shore-
ward transgression. These facts are evident in the Helderberg
regions of Maryland, Pennsylvania and eastern New York, close
upon the Appalachian heart, and confirmed by the sands of the
extra-Appalachian regions of western-central New York, Ontario
and Illinois.
We may have been disposed to believe that the typical fauna of
these early sands in America, which in this place we may char-
acterize as Oriskany, an assemblage made distinctive by its heavy
shelled brachiopods, Rensselaeria (ovoides group), Hipparionyx,
Leptaenaventricosa, Spirifer (arenosus type) and species of the
Spirifer murchisom group, large Leptostrophias, Plethorhynchus,
Leptocoelia flabellites, etc., gastropods of large size (Diaphorostoma
ventricosa and many capulids); these and their less conspicuous
associates were normal to these shallow waters; but there is good
evidence that the fauna of the sands and their shallow waters were
actually adjusted by slow adaption from the deeper waters of the
lime bottoms. This proposition would always be reasonable under
general conditions — the creeping of a deeper water fauna shore-
wards; it is specificaily indicated by the conditions in the north-
eastern Appalachians of Gaspé. One must bear in mind that in
respect to tectonic age these northeastern Devonic mountains are
the earliest of the entire chain; the Appalachian folding was begun
here and proceeded thence southward. In direct semblance to the
relative age of these Gaspé folds are the heavy limestone beds
of the Grande Greve formation in whose profuse fauna are the
I2Z20 NEW YORK STATE MUSEUM
‘species above listed, abounding in full address, companioned by an
entourage which, in part, elsewhere accompanies the Oriskany, but
also in part showing forth the Helderberg fauna in the dress of
later evolution. Here, I take it (and have endeavored to give the
demonstration in full) in these lime seas this northern Oriskany or
sandstone fauna of Appalachia took its origin and thence it traveled
southward through the open rias of that ancient coast into the
seas within the Appalachian barriers. Here, then, was a wide open
channel inward, in the northernmost of these Appalachian passages,
and with the inward movement of the fauna came its differentia-
tion and slow adjustment to the shoal waters.
In obvious contrast to this southwestern movement of the true
Appalachian Oriskany faunas was the migration through the parallel
channels of this northeast region lying farther to the south, one
where now the Bay Chaleur indents the Gaspé coast and perhaps
along others which lay between this and that equally ancient passage,
the Bay of Fundy.
These are indicated by the wholly arenaceous early Devonic beds
stretching across the state of Maine from Aroostook county on the
east through Piscataquis and Penobscot counties to Somerset on the
west. In all these shallow water channels there is a persistent and
well-defined element of the Coblentzian faunas which enforces the
contrast between them and the normal or standard Oriskany of
New York.
The case of the Gaspé sandstone. The Gaspé sandstone is a
unit of still somewhat uncertain limitations in stratigraphy, though
its base is definitely understood and lies at a small unconformity
with the Lower Devonic limestones. This evidence is taken wholly
from the thinned northern edges of the sandstone mantle on Gaspé
bay. Southward the horizontal development of the sandstones is
apparently and perhaps, in places, obviously continuous in their
upper part with the lower masses of sand and conglomerate which
enter into the composition of the formation on the Gaspé peninsula
known as the “ Bonaventure,” a term which appears to be correctly
interpreted as Devono-Carbonic, in the sense that it embraces
locally and throughout the region of its typical developments from
Bonaventure island southward, a series of essentially continental
deposits unconformably succeeding the marine Middle Devonic.
The Gaspé sandstones of Gaspé bay contain a marine fauna which
carries certain Oriskany species, Rensselaeria ovoides (gaspensis),
Eatonia peculiaris, survivors of the Grande Gréve fauna beneath,
but the majority of species in the assemblage, the pelecypods and
REPORT OF THE DIRECTOR IQI4 [21
gastropods particularly, have specific resemblances and indentities
with the described species of the Hamilton (Middle Devonic) sand-
shales of New York. I have so interpreted them. The sugges-
tion, however, has been made by Professor Williams that the
species of pelecypods find striking semblances among the species
of the Coblentzian. We may be sure this is so, for there
are similitudes running throughout the pelecypod faunas of
the Devonic which are actually a hindrance rather than a help
to the determination of specific values. I think, however, that the
careful consideration of the Gaspé sandstone marine species can
leave no doubt of their later than Oriskany age, even without the evi-
dence from the stratigraphy. Then, further, as long ago shown by
Logan and in detail by Dawson, these sandstones on Gaspé bay carry
a profuse terrestrial flora of unquestionable Middle Devonic age. We
have then here in the Gaspé bay region the singular phenomenon of
a highly calcareous “ Oriskany ”’ whose lower beds carry the typical
species of that fauna and in whose higher limestones there are
still commanding representations of the fauna with additions of a
later (Onondaga) type, followed above by heavy sands wherein are
still surviving species of the Oriskany, themselves autocthonic, but
enmeshed in an assemblage of post-Oriskany and post-Onondaga
age. The fact is that with the introduction of the Gaspé sandstone
begins the deposition of a widespread delta on whose outer fringe
only, here and there, has a rather depauperated marine fauna been
able to subsist, while the shoreward beds received the cutwash of
the land with its debris from the Devonic jungles. The evident
adjustment of the “ Oriskany ” species to a gravelly bottom and in
their proper place in the succession, is shown, for Gaspé, in a single
known band in the Percé cliffs.
The extraordinary concurrence of the primitive Appalachian
topography of the Maritime Provinces with that of today. The
bays and endroits of the present Gaspé coast, like the bays and
shores of Nova Scotia and Cape Breton, are the synclines and
flanks of the Appalachian folds. Overridden in part by horizontal
deposits in the late Devonic, the Carbonic and Permic of post-
Appalachia, they have come again above the waterline by elevation
and erosion and now conform the coast line and the continent to
their ancient curves. The apparent return after the ages to the
forms of so distant a past is in northern Gaspé not that, but the
simple retention of the original form. Gaspé bay lies in a syncline
as old as the Appalachian system and, in less degree, so do the
I22 NEW YORK STATE MUSEUM
larger rivers and their barachois. There is probably no other region
where so ancient a topography is still in so obvious-control.
The southward spread of the sand transgression. Of the lime
seas of the opening Devonic in regions which bounded the broken
Siluric lands of northern South America, we have no knowledge.
The basin of the Amazonas is sheeted with Devonic sands that lie
close upon the Siluric limestones. The sand deposits of the Rios
Maecurt, Ereré and Curua are not far away from the Siluric lime-
stones of the Rio Tapajos, and nowhere do we know aught of the
lime sediments which represented the deeper deposits of these
marine waters. They are absent or lie buried; probably the latter,
for the sands are without evidence of continental character. The
Maecurut sandstones are sufficiently abundant in species to indicate
their part in the great sand transgression of the opening Devonic,
but the; specific .characters of this fauna are not such as to knit
them closely with Oriskany faunas of the northern continent. There
are the differences which have resulted from distance, from divid-
ing land and submarine barriers, from isolated evolution in embay-
ments or basin seas; there are still the occasional indentities of
species, more often of distinctive genera, and, all told, in the
Maecurt sandstone an evident relationship in kind and time to the
Oriskany-Onondaga of the north. To the German geologist,
schooled in the Devonic of his own country, they are “ Coblentzian ”
and have been so termed, with reason, by Doctor Katzer; but they
are not adequately characterized by such a term; even less so than
by the terms of the North American succession.
From this Amazonas basin northward, Professor Schuchert
would disperse the fauna into North America by way of the Gulf
of Mexico embayment to connect with the Camden chert Oriskany
of Georgia. My own impression is that both the Maecurt and the
Camden “ Oriskany” sediments represent, by their faunas, embay-
ments from a continental strand line which had connection with the
north by way of the Appalachian channel seas, or perhaps, with
even more probability, with an outer shelf strand now submerged
with so much of the eastern-shore Appalachia.
We have recent knowledge of an extension westward of the
“normal” Oriskany fauna of New York into a pure white lime-
stone in St Genevieve county, Missouri, beneath it lying a well-
defined Helderberg fauna. This discovery carries the distribution
of the Oriskany farther in this direction than was before known.
Thence to the Camden cherts of Georgia is a distance so short as
to make, to express it in terms of paleogeography, but a narrow
REPORT OF THE DIRECTOR I9QI4 123
barrier between these deposits. But the faunas in these two approx-
imate points are still so unlike that to infer a junction of the waters
across the isthmus is not yet justified. Should it so turn out that
the Oriskany strand was here unbroken, we should then have the
fauna completing an entire circuit in Appalachia. The St Genevieve
basin at the west seems to present the duplication of the conditions
in the northeastern lime basins of Gaspé, an essential exclusion of
the sand from the contemporaneous deeper water. But we know
too little yet of this Missouri basin to institute any satisfactory
comparison between its Devonic elements and those of the northeast.
To return then to the Brazilian fauna of the Maecurt river sand-
stones, we may feel reasonably secure that its distance from the
overspread of the northern sands, the opportunities for variations
from those faunas by development under conditions of isolation,
are the responsible factors for actual and apparent differences in
these faunas from those of the north.
It will not do, however, to intensify these differences by statement.
The affinities are obvious and they are distinctive in generic char-
acters. In a certain sense there is in comparison with the northern
Oriskany, a later tinge to the fauna; species which carry suggestions
of the stage next succeeding in the New York succession. This
is entirely in accordance with such expectations as we should derive
from our knowledge of the Brazilian sections, for the next term
above the Maecurt: is the sandstone of the Rio Eréré, and its
fossils, as described by their discoverers, Hartt and Rathbun, and
confirmed by the evidence brought out by Derby and myself, indicate
their Middle Devonic age and their rather intimate relations with the
Hamilton of New York. The intermediate limestone term of the
series present in the New York succession is then missing here,
with our present knowledge, but the open and freer connection of
this later shallow sea with the northern seas of the Middle Devonic
is a very pronounced fact. In speaking of the Gaspé sandstone
fauna, I have referred to Professor Williams’s intin.ation that its
pelecypods might be construed as Lower Devonic (Oriskany-
Coblentzian), and I may here refer to Doctor Katzer’s contention
that the Eréré sandstone fauna is likewise Lower Devonic. The
two suggestions are not alike in quality nor based on like argumenta-
tion, though similar in purport. Yet with close analysis of these
faunas we are not prepared to concede these alternative propositions,
even though at the south, the later Ereré sandstone is in direct
continuity with the earlier or Maecurt. At all events, the specific
and generic similitudes of these two Amazon faunas with those at
124 NEW YORK STATE MUSEUM
the north, greater in the later (Eréré) stage than in the earlier
(Maecurtt), cease and determine at these latitudes.
The austral faunas of Brazil, Argentina and the Falkland
islands. The employment of the term austral, which I have used
before as an emphatic distinction from the boreal faunas, means
that in these regions under consideration and in Cape Colony as
well, in other words, throughout the higher latitudes of both
southern continents, there is a palpable and fundamental difference
from the boreal faunas. The fact may well be stated with emphasis,
but not to the exclusion of certain common bonds which declare
the age of the faunas. It is well known now, was stated by Stein-
mann, A. Ulrich and Knod for Bolivia and corroborated by my own
somewhat protracted researches upon materials from Sao Paulo, the
Argentinian Cordilleras and the Falkland islands, that, in terms of
biology, there is no Devonic in these southern latitudes except the
early Devonic. Whatever the thickness of the sedimentation may be
(unknown now) and whatever its lithology, it is all of an age
which corresponds in paleontology to the early Devonic of the
north. Whether the duration of deposition here does or does not
represent only that of the northern Lower Devonic or that of the
entire northern Devonic, it is perfectly clear that the fauna is one
fauna and endured from the beginning to end of marine Devonic
deposition. If there may have been a series of later Devonic faunas
in these regions, we must say either that they were cut out by
geography or cover our ignorance in the buried rocks. Professor
Kayser, writing on some of the spirifers from Tibagy, in Sao Paulo,
was among the first to indicate the quality of the Brazilian fauna,
and the work of A. Ulrich and Knod in Bolivia has added con-
firmation to the interpretation of this Devonic.
Now that we have assembled the fauna of all these regions in
reasonable fulness, the conclusion regarding the time equivalence
of the entire austral fauna stands out with clarity. The Falkland
sandstones, the Tibagy sands, the Sao Pauio lime muds, the sands of
Argentina are variations in sedimentation whose exact relations
in stratigraphy are not yet known, but which are knit together by
a common biology. An obstacle to the solution of the real character
of the paleontology here has been the natural impulse on the part
of students in this field, bringing to their interpretations an acquaint-
ance with the boreal Devonic, to enforce parallels and identifications
of southern with northern species —to squeeze the unknown into
the moulds of the known —a customary and often an almost im-
perative procedure.
REPORT OF THE DIRECTOR IQI4 125
The composition of this austral Devonic fauna, on close analysis,
brings out the evident fact that, whatever its origin, it has developed
its peculiar characteristics under the influence of isolation from the
other Devonic basins and shelf-seas of this stave. In South Africa
it may be demonstrable on further evidence that the same fauna
was preceded by a period of continental deposition properly included
within the Devonic system. But in either case there is no indication
that the primary calcareous term of the northern Devonic, by its
absence in the south, is to be regarded as a factor of any weight
whatsoever in estimating the relative stage of the austral fauna. In
the Falkland islands, where the affiliations of the marine fauna are
more intimate with that of the Bokkeveld beds than with the nearer
South America fauna, there fails as yet any evidence of a pre-
liminary Devonic deposit of continental character.
These extensive and reasonably profuse faunas of the southern
Devonic strands developed -along a continent obviously separated
from that at the north, and for most of its extent widely by equa-
torial Atlantic waters, but narrowly in the subequatorial latitudes
of Brazil, where the Amazonas faunas, with affiliations toward the
north, lie not far away from the Devonic beds of Matto Grosso with
evident alliances with the south. The marine Devonic was the
strand of a Pre-Gondwana land of whose constituent sedimentary
rocks we know little save for the occasional dredging of altered
sediments from the Atlantic bottom, the gneissoid inclusions in the
deep-seated lavas of the mid-Atlantic islands, and perhaps some
part of the crystallines of the southern islands, South Georgia, the
South Shetlands and of Antarctica. To these are to be added the
South African premarine Devonic series capped by the Table
Mountain sandstone, now regarded by some writers as of glacial
origin, and, of course, some part of the Precambric crystallines of
South America and Africa.
Our present knowledge leads us to the conception of an Andean
Siluric and Cambric land reaching far to the north along the
Cordilleran rib, for the limestones of eastern Argentina, Bolivia and
Peru carrying Liorhynchus bodenbenderi and its associated fossils,
are Siluric, not Devonic. The stretch of the Devonic strand along
the Cordilleran rib far to the north is now well known and there is
every reason to believe that the Pre-Gondwana land which traversed
the south Atlantic extended an arm well to the north on the Pacific
side. Pre-Gondwana land was thus a very ancient austral con-
tinent, and wholly comparable in extent and age to Laurentia at the
north. The latter, in days before the Caledonian folding, traversed
126 NEW YORK STATE, MUSEUM
the north Atlantic basin, just as the former, perhaps more insulated
but of wider extent, stretched across the south Atlantic from south-
west northeasterly.
Problem of the black shales. The Upper Devonic of Appalachia
is eminently characterized by its abundance, often preponderance,
of black shale beds. These are thickest in Michigan, Ohio, Ten-
nessee and Kentucky and seem to thin *continuously eastward into
New York. Not all students have agreed in construing the entire
heavy mass of these bituminous shales as Devonic, but the upper
divisions (Chattanooga shales) have been, with some reason, as-
signed to the opening stage of the Carbonic. It is probably true
that these shale bands have been studied most closely in New York
where it is evident that they represent the thinning edge of the body
of this sediment. Here the upper black shales of the Genesee and
Portage groups have caught more abundantly than elsewhere the
characteristic marine fauna of the intercalated deep water marine.
A customary interpretation of the origin of these black Devonic
shales 'was that of shallow water origin. This conception assumed,
largely on the basis of the plant remains in which the rocks abound
and especially the accumulations of sporiferous deposits occurring
in the Ohio beds, that they were near-shore beds formed in shallow
basins with choked outlets. Another popular explanation was to
refer them to the accumulation of fat muds beneath a Sargasso sea.
Both interpretations, twenty years ago, were accepted alternatively
without special scrutiny. At a later date the writer had occasion to
give attention to the problem and in seeking a solution brought out
the very evident fact that the known seaward sweep of terrestrial
vegetation by rivers of the land into the rivers of the ocean, the
abundance of such distant flotsam observed by oceanographers,
failed to compel any such interpretation as the first, while the
Sargasso sea conception is entirely eliminated by the nature of the
flora of these shales, which is wholly terrestrial. The Genesee and
Portage black shales, furthermore, were shown to carry a highly
characteristic marine fauna, whose elements show a deep water
habitus.
These older conceptions have the merit of the obvious and
specious. There are, however, deeper considerations which have
been brought out with some degree of analytical force and which
are not in harmony with this interpretation of a shallow water
origin for these extensive deposits. If I am not mistaken, it was
Professor Williams who first directed attention to the fact that in
all the bituminous shale beds of the Appalachian Paleozoic succes-
REPORT OF THE DIRECTOR IQI4 127
sion — the Utica shale of the Ordovicic, the Marcellus of the Middle
Devonic, and these Genesee-Portage shales of the Upper Devonic
—there is throughout a common character in tne aspect of the
contained marine fauna. Deficiency of lime makes ali species thin
shelled; all species are of rather depauperated size, phosphatic
brachiopods (Lingula, Orbiculoidea etc.) abound while the lime-
shelled species are few, small cephalopods are frequent while other
Mollusca are rarer and fragile. The statement is only a natural
expression of the effect of like conditions on various faunas.
1 The faunas of the Genesee-Portage are strictly marine;
2 They are, taken as a whole, of the deep water type whi.h em-
phasizes the Portage fauna in its highest development (Intumescens
fauna) ; indeed, they represent this fauna;
3 The shales carry a thin lime deposit, continuous over a great
extent of latitude and essentially a mass of pteropods. I have in-
dicated that this Styliolina or Genundewa limestone holds the ptero-
pod Styliolina in numbers of 50,000— 100,000 to the cubic inch.
By analogy these minute creatures are pelagic open sea animals.
These limestones, too, carry the Intumescens fauna in a typical
though prenuncial development ;
4 The shales abound in exudations of FeS,; indeed, the base of
the Genesee shale in western New York rests on a continuous layer
of pyrite extending for 100 miles and carrying the relicts of a fauna
(Hamilton) dismally dwarfed by the foul conditions which it hope-
lessly tried to survive.
These features of the fauna and their physical surroundings I
have found illuminated by the parallel conditions prevailing in the
depths of great inclosed seas like the Mediterranean and the Black
Sea, where limeless waters, free liberation of sulphur in connection
with a rapid organic decomposition under great pressure, are pro- -
ducing such foul bottoms with sulphide compounds, dwarfed and
thin-shelled Mollusca, always, of course, with the accretion of what
may fall in from flotage and dying pelagic life. These inferences
as to the deep water origin of the black shales are corroborated by.
their greater thickness westward of New York.
In extraordinary contrast to these conclusions is the proposition
put forward by Professor Grabau that the bituminous shales are
delta deposits, brought in by a putative southwestern river flowing
northeasterly, discharging this singular supposed fluviatile-con-
tinental mass over an area of many hundreds of square miles. This
view seems to the writer the extreme expression of a recent obvious
tendency to magnify the part contributed by alluvial floors and fans,
desert desiccation and other continental factors to the upbuilding of
the geological column. .
128 NEW YORK STATE MUSEUM
The Old Red Sandstone. The conception of these beds as to
origin is now rather definitely formulated. Through years of waver-
ing interpretation we have reached a point at which we may concede
the essential continental origin of most of the deposits which may
be fairly embraced under the designation above employed. The:
force and proof of this conception is largely due to the effective
work of Professor Barrell, who has attacked the problem from an
angle new to the usual approach. The Catskill formation of the
Appalachians and the Oneonta sandstone which lies at or is con-
tinuous with its western base, are, according to this interpretation,
the outwash or delta plains composed of the debris of the more
easterly lying mountainous lands, now either completely lost beneath
the eastern sea or represented only by their metamorphosed roots.
I think that for the interpretation of these great delta plains
fringing the interior sea of the Upper Devonic, too little emphasis
has been laid on the tremendous mid-Devonic mountain making all
through the northern Caledonid Appalachians — a time of orogenic
revolution which greately overpassed in energy that of any other
period in the history of the mountains. With the opening of late
Devonic time, all through this region there were the newly made
mountains rising to fresh heights and inviting the most vigorous
attack of meteoric waters; inviting, too, as a natural consequence,
the formation of such tremendous plains of continental debris all
along the shore lines.
There must have been on the now buried eastern shores of Appa-
lachia, deltas of similar origin and extent to those we now know on
the western shores. While the general proposition is a closed one
and we may find satisfying explanations of all the phenomena pre-
sented by the accumulation of continental material on the edges of a
marine basin, with all necessary accompanying phenomena of inter-
digitation of deposits, local repulse and invasion of marine faunas,
etc., there still remain some open questions as to the scope of the
continental factor, in time, and as to its exclusiveness in effect.
Does the Catskill formation, in its typical development in the
Catskill mountains of New York, represent exclusively Devonic
sedimentation, or does it transcend the Devonic boundary? As-
sumption commonly favors the former, but there are outside evi-
dences that indicate the latter presumption, drawn from a con-
sideration of the Bonaventure conglomerate.
Bonaventure conglomerate. This mantle of sandstone and
conglomerate sheets the present coasts of the northern Mari-
time Provinces of Appalachia, seldom extending inland in its region
REPORT OF THE DIRECTOR IQI4 129
of typical development. It was commonly regarded by earlier ob-
servers as lying unconformably on the Gaspé sandstones and by
Logan, who first described and named it, as a Carbonic formation.
I have made reference already in speaking of the Gaspé sandstone,
to the presumable horizontal continuity of the two, the upper beds
of the former with the lower beds of the latter, intimating thereby
no interruption of deposition though with an evident change of
coast line and drainage.
In fact, in this respect, in the northernmost extent of the Bona-
venture formation and the southernmost of the Gaspé sandstone,
the relations presented are similar to those of the early Catskill
stage and the marine Devonic (Ithaca) of the westward seas. In
southern Gaspé and thence into the lower gulf, the Bonaventure lies
everywhere atop of the almost vertical Siluric-Ordovicic limestones
and, in places, on the equally upturned Lower Devonic. So here
again in this Bonaventure formation is the evidence of great land
waste from the folded early Devonic mountains, obviously from a
land eastward of the present coast. The conglomerates of the
Bonaventure carry fossiliferous pebbles and boulders of all the
earlier formations, those of the Lower Devonic being of greatest
abundance, but with exception of these last the boulders are largely
from beds unfamiliar to the present land. I am not yet satisfied
that any of these boulders which have come under my observation
are ice-scratched, but many of them are very large and occasionally
one will weigh several hundred pounds. Indeed, Sir William Logan
records one of them which weighed a ton. We are not justified
yet in appealing to the action of any other agencies in accumulating
these, except continental water and shore ice with the addition of
the work that would be done along the higher coasts of the moun-
tains, on its headlands and promontories by the pounding of the sea.
To the latter I believe we must ascribe a definite part in the work of
building the formation. ;
The evidence that the Bonaventure transcends Devonic time is |
largely negative; it lies on no fossil evidence, though plant remains
of still undetermined character are scattered through the sand beds.
But in this region it represents all the rest of Paleozoic time that is
recorded by the rocks, and what part of the piie may be Carbonic
must be determined from the study of the still little known ac-
cumulation of this continental waste which sheets New Brunswick.
At Migouasha or Scaumenac bay at the head of the Bay Chaleur,
there is a different expression presented in the gray and more cal-
130 NEW YORK STATE MUSEUM
careous sand cliffs carrying the extraordinary profusion of Ostra-
coderm and Crossopterygian fishes and beautifully preserved ferns.
The plants are natural land wash while the fishes are presumably
the natives of the stream mouths, probably migrant into the fresh
waters for spawning purposes, like the salmon which today maintain
this historic procedure in the streams which traverse these rocks.
Beneath these remarkable cliffs is a°gray boulder shale whose
boulders are more largely of the fossiliferous limestones and less
of the crystallines than in the Bonaventure. We are not yet pre-
pared to be positive regarding the origin of this underlying boulder
shale. Its matrix resolves easily to clay and squeezes out over the
landwash, setting its boulders free. Its component blocks are frac-
tured, impressed and ice-scratched. The students of the fish-bearing
Magouasha beds above are quite in accord in regarding them as of
Upper Devonic age, though this conclusion has not as yet full con-
firmation from the other biotic elements.
The late Doctor Ells found evidence satisfactory to him of an
unconformity within the mass of the Bonaventure conglomerate
which was assumed to divide the time of its deposition by a slight
diastrophy. If this interesting division can be fully demonstrated,
it establishes a very noteworthy agreement with the Old Red of
northern Scotland which is marked by a widespread disconformity
of this kind.
Origin of the Intumescens-fauna. It was essentially with the
help of Professor Kayser’s studies of the “ Intumescens fauna ” of
the Upper Devonic, that the writer prosecuted his investigations of
this fauna in America. The “ Tntumescens-fauna ” of the Genesee-
Portage stage has proved to have had a profuse and highly char-
acteristic development in western New York, though quite suddenly
losing itself thence in all directions. Eastward its place is taken
in contemporaneous strata by the brachiopod faunas of the Ithaca
and Chemung groups, so that no evidence of its existence is to be
found on the western shores of old Appalachia. Westward traces
of it are found here and there, in Iowa, in Manitoba, a striking
development in Montana. The fauna, it was claimed by the writer,
took its origin from the region of its great development in northern
Siberia (Timan), and its dispersal was eastward along American
strands into the interior sea of early Upper Devonic Appalachia
where, favored by its isolation, it burst out into a fulness of de-—
velopment. Professor Schuchert, in the construction of his paleo-—
geographic maps, has felt it necessary to introduce this fauna from
REPORT OF THE DIRECTOR IQI4 131
the east through a putative passageway across Appalachia, in
northern New Jersey. Paleogeography makes many tentative de-
mands ‘of its followers. The writer could never visualize this
gateway and Professor Barrell, after long study, has hung over it
the. sien.7.°,.Clasedv?
The extent of Devonic intra-Appalachian vulcanism. Outside
the western hemisphere, volcanic activity was widespread during
the early Devonic. The interior Devonic basin of North America
has been regarded as almost devoid of such activities and, from
South America, we have no present knowledge of volcanic out-
flows in the sheet of Devonic sediments. The contrast in this regard
between the basins or intermontane channels of the northeast Ap-
palachians and those farther south is very marked. Rhyolitic ashes
and scoriae interlaminate the marine Lower Devonic of Dalhousie;
volcanic dikes traverse the lower limestones on the Grande Greve
peninsula; the Gaspé sandstone is cut in several places by such
dikes and the Bonaventure formation is locally overwhelmed by
lava outpours. New York and the interior region are not wholly
without such evidences— dikes of alnoite penetrate the Upper
Devonic near Ithaca, serpentinized peridotite forms dikes which
traverse the Siluric and Devonic about Syracuse; dikes of like
character, in an extensive parallel series, cut the Ordovicic of the
Mohawk valley and may have penetrated, in all probability did, a
once overlying Devonic mantle. These dike intrusions; however,
are along preexistent fault or joint lines, all accessory to the orogenic
structure of the eastern mountains. In other forms than this, vul-
canism, it has been generally regarded, does not manifest itself in
these Devonic areas of the interior.
Over the St Lawrence lowlands lying between Montreal and the
New York-Vermont boundary, is an array of volcanic stacks and
domes varying in size and effect from the most majestic in Mount .
Royal, to the lesser ones at the south; all of which have been termed
by Doctor Adams, the “ Monteregian Hills.” These are lavas in
_ various stages of differentiation but all have obviously penetrated
a great plain of Ordovicic (Lorraine) shales. There is, however,
a definite indication of the age of these intrusions presented by the
contact breccias known on St Helen island near Mount Royal, in
which are fragments bearing unquestionable Lower Devonic fossils;
fixing thus the age of the lava intrusions as at least post-Lower
Devonic. These blocks in the breccia are the only known trace of
the Devonic in all this region, from the St Lawrence southward into
132 NEW YORK STATE MUSEUM
the mountain folds of New Hampshire, and the inevitable con-
clusion is before us of their former existence here and present
almost total destruction.
Quite outside of this Monteregian province (‘a petrographic
province,’ Adams), about 150 miles to the south within the State
of New York, lies the volcanic plug known, from its historic asso-
ciations, as *‘ Stark’s Redoubt.’ This volcanic mass, very limited in
width and extent, has been the subject of much study and discussion.
Apparently it is a basic pillow lava, deeply serpentinized and having
the aspect of a kimberlite with a surprising amount of free carbon.
It seems to be interbedded with “ Hudson River” shales which at
this point are of Ordovicic age, but the mass is sheared and the
shales faulted against it and there is little doubt that the lava tran-
sected the lower part of the shale beds. In our present knowledge
of the former extent of the Devonic rocks, in New York at least,
beyond their actual outcrops; our necessary admission of their re-
moval over tremendous areas by ice erosion; in view of such evi-
dence of great loss as is brought out by the arctic distribution of
these rocks (see next caption), and, for specific example, by the
great upstanding edge of the Helderberg escarpment in New York
whose abruptly cut-off edges face the great north where once its
undiminished sheets of strata must have extended but where today
no trace of Devonic has survived; such evidence approves the con-
ception that the “ Stark’s Redoubt” volcano, like the Monteregian
Hills, is of like origin and date — not earlier than Lower Devonic,
and like them a manifestation of the igneous intrusions and out-
pours which characterized the Caledonid type of Devonic orogeny.
A world of knowledge regarding the distribution of Devonic seas
and faunas awaits us from both Arctic and Antarctic America. No
fields, perhaps, are left where so important clues are buried and
though these lie under a grievous load, they nevertheless beckon
most alluringly to the hardy spirit. The suggestive geologic data
brought away from Antarctica first by Eights of Albany and more
than three-quarters of a century later by Shackelton and the
lamented Scott forecast the light from these Cimmerian latitudes.
The remarkable collections gathered from Arctic Ellesmere-land by
Doctor Schei of the second ‘“‘ Fram” expedition, intimated an extra-
ordinary development of Appalachin Devonic in the high north
REPORT OF THE DIRECTOR IQI4 133
Meyer, Loewe and Holtedahl, who have worked out the paleon-
tologic factors of this Devonic succession, have demonstrated a
highly developed series beginning with an actual representation of
the calcareous members, the Keyser (or introductory unit of the
Maryland succession), the Coeymans and New Scotland members
of the Helderberg, and so on upward with a final Devonic member
carrying terrestrial plants in a continental sediment.
These important discoveries compel us once more to reconstruct
the paleogeographic map, for the most obvious conclusion derived
from these data is the direct and immediate connection of fairly
deep arctic marine waters with the interior seas of Appalachia.
_ The Siluric bay, which has been made to reach its long way south-
ward from the Arctic into the interior and has been conceived to
have brought thence its faunas, reached up rather than down, and
its waters were not shrunken at the close of the Siluric by a northern
positive movement of the land. Palpably, as Doctor Meyer has sug-
gested, the Devonic water way to the north must have been wide
open all about these western and northwestern shores of the great
Laurentia; and if the Devonic strata fail to appear there in the
interval between New York, southern Ontario and Ellesmere-land,
it is either because their remains still lie unrevealed or have been
swept away by heavy erosion.
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NOTES ON TEE INTRAFORMATIONAL CONTORTED
ot kei AAT TRENTON @AELS
BY WILLIAM J. MILLER
INTRODUCTION
In 1908 the writer published a short paper in the Journal of
Geology * describing the contorted strata within the Trenton forma-
tion at Trenton Falls in central New York and offering an ex-
planation of the phenomena.
Recently (1913) there has appeared an elaborate paper by the late
F. F. Hahn in the Neues Jahrbuch fur Mineralogie, Geologie und
Paleontologie* in which the contorted strata at Trenton Falls are
particularly discussed and an entirely different explanation is offered
for the phenomena there, as well as for apparently similar phenom-
ena in certain other parts of the world.
Grabau * (1913) discusses the contorted zones at Trenton Falls
and similar phenomena elsewhere and fully accepts Hahn’s explana-
tion, but he neither states nor presents arguments against the present
writer’s hypothesis.
It is not the present purpose to consider intraformational cor-
rugations in general, but rather to confine attention to such features
as are to be observed at Trenton Falls. It will be shown that
Hahn’s explanation can not apply there. It is generally agreed that
intraformational contortions may be produced in several ways, and
the present concern is to find the correct explanation of the cause
of the particular phenomena at Trenton Falls. For certain details
not repeated in this paper, the reader should consult the two papers
above cited.
THE CONTORTED ZONES WITHIN THE TRENTON FORMATION
Excellent examples of highly folded or contorted strata between
nonfolded strata may be seen along the sides of the gorge at
Trenton Falls where the disturbed beds occur at two very distinct
1 Highly Folded Between Non-folded Strata at Trenton Falls, N. Y. Jour.
Geol., 16: 428-33.
2Untermeerische Gleitung bei Trenton Falls (Nordamerika) und ihr
Verhaltnis zu ahnlichen St6rungsbildern: Neues Jahrbuch. 36: 1-41,
1913.
3 Principles of Stratigraphy, p. 783-84.
136 NEW YORK STATE MUSEUM
horizons within the Trenton limestone. The lower contorted zone,
whose base lies 144 feet below the top of the Trenton, is from
4 to 6 feet thick. It is visible only near the crest of the lower part
of the High fall (see accompanying plate) and in the upper end
of the gorge near Prospect village where the strata are highly in-
clined. The upper contorted zone, whose base lies 65 or 70 feet
below the top of the Trenton, is from about 5 to 12 or 15 feet thick.
It is well exhibited along the path opposite High fall from which
point it may be traced along the sides of the gorge for nearly 2 miles
to Prospect.
The impure limestone layers of both the folded and nonfolded
portions average only a few inches in thickness and are separated
by thin bands of shale. Within the folded zone horizons the layers
are, in some cases, scarcely folded or broken; sometimes they are
gently folded or tilted; while most commonly they are highly folded
and fractured (figure I).
Fig. 1. The upper contorted and broken zone as
seen along the footpath opposite the crest of High
fall at Trenton Falls. Drawn from nature.
Numerous observations show the strikes of the contorted zone
folds to be from N. 50° E. to N. 65° E. or practically parallel to the
strike of the distinct folds in the Trenton formation in this region,
as well as parallel to the strike of the well-defined fault-fold line
passing through the village of Prospect (see geologic map).
It should also be noted that these contorted strata occur only
in a very local district. As far as they can be ascertained they are
1The interested reader should consult the writer’s geologic map of the
Remsen quadrangle in N. Y. State Mus. Bul. 126.
S]J@4 UojusTy ye Wey YsizZ fo sed
JIMO]T 9Y} FO JsotID oY} IWIU UI9S Se 9UOZ UdYOIG PUL Pd}10JUOD IOMO]T IT
ojoyd “OF4AN “DL
REPORT OF THE DIRECTOR IQI4 137
visible only in the Trenton Falls gorge and in the bed of Cincinnati
creek 1% miles southwest of Prospect.
HYPOTHESES REGARDING THE CAUSE OF THE CONTORTIONS
Tectonic hypothesis. The explanation offered by the writer is
that the contorted zones were produced by differential movements
within the mass of the Trenton limestone. The displacement
(140 feet) of the thrust fault at Prospect village was sufficient to
cause the beds of the-middle Trenton to slide over beds of the
upper Trenton. Near the fault-surface the strata on the upthrow
side are bent upward at angles of from 30 to 4o degrees. Figure 2
shows the relation of the folded zones to this fault.
ON FOSS RRR GBR
eZ Se RB
SS L LLL
RS pI poe
Se ae ee in es SOOT! SIDI aanamanaae
Cc D E
if SCALE
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Fig. 2. Section showing the position of the two corrugated zones within
the Trenton formation and their relation to the thrust fault at Prospect,
near Trenton Falls
It is easy to see how, when the force of compression was brought
to bear in the region, the higher Trenton beds on the upthrow side
must have moved more easily and consequently faster than the
lower Trenton beds. For instance, the portion A in figures I and 2
being separated from C by an intermediate mass B of possibly
slightly less rigidity would slide over C and cause the portion B
to become ruffled or folded and fractured. Occasionally parts of
zone B would be moved very little or would be moved along with-
out being folded. The portion B would need to be only very slightly
less rigid than the adjacent portions. The somewhat thinner lime-
stone layers separated by thicker shale partings would cause the
part B to be thus less rigid. A similar explanation applies to the
lower folded zone, and the folded or contorted zones thus merely
indicate horizons along which the differential movements have taken
place.
138 NEW YORK STATE MUSEUM
Some of the points favoring this tectonic hypothesis are as fol-
lows:
1 The very existence of the thrust fault at Prospect and the
distinct folds in the Trenton formation just to the south make it
certain that there must have been differential movements within the
mass of the formation.
2 Contorted zones are known to have been produced by differ-
ential movement of more resistant beds over weaker beds in various
regions of folded rocks (for example, Marquette district of
Michigan).
3 The parallelism of the strike of the folds of the Yrentes
formation with that of the fault at Prospect.
4 The parallelism of the strikes of the small folds and faults
of the contorted zones with the strikes of the larger folds and
the fault at Prospect.
5 The limitation of the contorted zones to the upthrow side of
the only considerable thrust fault in the Paleozoic rocks of central
New York. |
6 The absolute limitation of the contorted zones to two very
definite horizons in the Trenton formation instead of there being
masses of disturbed strata irregularly distributed through the
formation.
7 The worn character of the upper and lower surfaces of the
contorted zones marked by layers of limestone sharply broken across
and the presence of numerous fragments of limestone.
8 The corrugations could not have been produced before deposi-
tion of the overlying masses because (a) the limestone. layers at
least were comparatively hard and brittle when contorted, as shown
by the numerous sharp breaks; (b) there is no evidence of very
irregular or crumpled upper surfaces of the contorted zones with
sediment deposited in the irregularities or depressions; and (c) any
attempt. to explain the contortions as due to slumping of masses
on the sea bottom is utterly opposed by the low angle and direction
of slope of the sea bottom as brought out below, and the remarkable
thinness and considerable extent (2 miles) of the contorted zones.
Q Experimental evidence clearly suggests the possibility of pro-—
duction of contorted zones by such differential movements.
Hypothesis of submarine gliding. According to Hahn, the con-
torted zones at Trenton Falls are excellent examples of phenomena
which have been produced by sliding or slumping of masses on a
sloping sea bottom during the process of sedimentation. The ac-
companying diagram (figure 3) will serve to illustrate the principle.
REPORT OF THE DIRECTOR IQI4 139
Fig. 3. Diagram illustrating Hahn’s hypothesis of submarine slumping
A lenslike mass breaking loose from any cause (for example, earth-
quake shock) would glide down the submarine slope and, because
of increased friction and water pressure and the striking of some
obstacle on the sea bottom, the gliding mass would come to rest
only after it had become considerably deformed or contorted, as
shown in the diagram. Sediments would then be deposited in
normal order over the crumpled layer. The most intense folding
would be toward the front of the transposed mass and of course the
strike of the folds would be at right angles to the direction of move-
ment of the sliding mass. Conditions for such submarine gliding are
regarded as favorable at many places along the marginal sea bottom.
Some of the points supporting this submarine sliding hypothesis,
according to Hahn, are as follows:
1 Observed production of contortions by subaqueous gliding,
for example, that in Lake Zurich 1875.
2 Various portions of the sea bottom are known to have slopes
of from 4 to 18 degrees or more which would be sufficiently. steep
for masses to slide down under certain conditions.
3 The texture (character) of materials within the contorted zones
is essentially the same as that of the underlying and overlying ma-
terials, and hence the disturbed zones were not horizons of weakness
which were distorted under pressure.
4 The analogy of the Trenton Falls contorted zones with those
of certain other regions.
5 Tectonic contortions are pressure phenomena produced under
heavy loads. : |
6 The corrugated zones are not of tectonic origin, that is, due
to differential movements within the Trenton limestone because
of (a) absence of stretched or flattened out masses; (Db) absence
of distinct slickensided or streaked surfaces; and (c) absence of
fragments of both the underlying and overlying masses within the
disturbed zones.
140 NEW YORK STATE MUSEUM
7 No clear drag or gliding zone is visible, but rather there is
often gradual transition between the contorted zones and the over-
lying strata.
DISCUSSION OF THE HYPOTHESES
Certain points not mentioned above as well as others requiring
fuller discussion will now be considered. It is not the purpose of
this paper to deny that, under proper conditions, subaqueous slump-
ing, with resulting contortions, may take place, but it is our concern
to show that the contorted zones at Trenton Falls do not admit
of such explanation.
An important fact, which in itself is well-nigh fatal to the hypo-
thesis of submarine slumping, is that the slope of the sea bottom
on which deposition of the Trenton beds took place was altogether
too slight. The writer has presented detailed evidence to prove
that, in the Trenton Falls district, the sea bottom receiving Trenton
deposits was remarkably smooth and with greatest slope toward the
southwest at the rate of only 6 to 20 feet a mile.t Similar evidence
for the adjoining Little Falls? and Port Leyden? districts by
Cushing and the writer show respective slopes of only 6 to 10 and
about 30 feet a mile. Considering a slope of 12 or 15 feet a mile
at Trenton Falls, this is 30 to 40 times less than the slope (4 to 6
degrees) in Lake Zurich, which Hahn cites as a remarkable instance
of very slight slope upon which slumping occurred. In fact the
floor of the Trenton sea in the vicinity of Trenton Falls was so
nearly perfectly horizontal that any such slumping or gliding of
masses, as required by Hahn’s hypothesis, could not have taken
place.
But, even if we grant the possibility of submarine gliding, an-
other difficulty stands in the way, namely, that the gliding masses,
as judged by the obvious criterion of strikes of small folds within
the contorted zones, must have slumped off toward the northwest
when, as a matter of fact, the greatest slope of the sea bottom was
at right angles to this, or to the southwest. |
Emphasis is placed by Hahn upon the fact that the materials of
the contorted zones are not notably different (weaker) than the
inclosing materials. While differential motions would certainly
tend to concentrate along distinctly weaker belts, such belts are not
deemed absolutely essential because the slipping once having even
1N. Y. State Mus. Bul. 126, p. 36.
2N. Y. State Mus. Bul 77, pos.
SING Yo State Migs. ale 135 ape
REPORT OF THE DIRECTOR IQI4 | IAI
a little start, as along two horizons within the formation, any
renewed or continued movement would tend to follow the same
horizons. It is at least significant that the contorted zones occur
in the weakest portion of the Trenton formation; that is, where the
soft shale partings are the most pronounced.
Replying to the statement that tectonic contortions are pressure
phenomena produced under heavy loads, it may be said that, in
the light of comparatively recent investigations, a great overlying
load would not be necessary in order to permit the development of
folded and faulted structures such as those in the contorted zones
at Trenton Falls, particularly since the strata are alternating thin
layers of unaltered limestone and soft shale. No doubt consider-
ably more overlying rock was present during the folding and fault-
ing process than now. Distinctly stretched or flattened out masses
would scarcely have been produced under the pressure conditions
which obtained.
In contrasting folds of the zones of fracture and flow, Leith
clearly states! that there is “little slipping between the beds” in
the zone of flow, while there is “ much slipping between the beds ”’
in the zone of fracture. The deformation of the strata at Trenton
Falls certainly took place in the zone of fracture as proved by the
very existence of the sharp thrust fault and the fractured character
of the rocks within the contorted zones. Considering also the thick
partings of soft shale, it is readily seen that the conditions were
very favorable for slipping between the beds or differential move-
ments of the strata.
Hahn also emphasizes the point that slickensides should be very
evident according to the tectonic hypothesis. While it is true that
some slickensides occur within the disturbed zones, nevertheless
they are not very evident at either the tops or bottoms of those
zones. When it is remembered that the Trenton consists of alter-
nating soft shales and comparatively hard limestones, it 1s easy to
see how the sliding must have taken place along the bands of soft
shale which were more or less crushed but not notably slickensided.
In spite of the lack of direct evidence from slickensides, the writer
believes that the multitude of sharply broken limestone fragments
(apparently not recognized by Hahn) toward the tops and bottoms
of the disturbed zones, as well as within them, clearly supports. the
view that there has been actual rubbing (sliding) of the masses of
the disturbed zones against both the overlying and underlying
masses. Even if we should grant Hahn’s argument concerning lack
1 Structural Geology, p. III.
142 NEW YORK STATE MUSEUM
of slickensides, this same argument applies against his own hypo-
thesis, at least as regards the under sides of the disturbed zones.
Thus, when the disturbance took place the limestone layers not only
were contorted but were hard and brittle enough often to break
sharply and rub over each other with occasional evidence of slicken-
sides, and it is quite reasonable to ask why the sliding of large
masses of relatively hard rock on the sea bottom took place without
leaving distinctly streaked or slickensided gliding surfaces.
The statement that instead of clearly defined drag (or gliding)
surfaces there is often gradual transition between the contorted
zones and overlying strata may be answered by saying (a) that the
writer's observations show rather sharp separation between the dis-
turbed strata and overlying undisturbed strata to be quite the rule
(see figure I and accompanying plate) ; and (b) that the few blocks
of apparently undisturbed rock within the horizons of the disturbed
zones are blocks which either were moved en masse without being
crumpled or they are blocks which may have moved relatively little,
if any, while the overlying strata slipped along. Blocks of this
latter class would have acted as local buttresses against which the
deformed layers may have piled up to thicken locally the disturbed
zones. Thus, along the footpath just south of the railroad bridge,
the strata seem to be in normal order; then passing southward, there
are masses of tilted and broken strata forming a zone of unusual
thickness (10 to 15 feet) ; and finally, just opposite the High falls,
the highly contorted and broken zone occurs with thickness of
5 to 8 at the same horizon. Such an arrangement of masses
within the horizon of a contorted zone is quite in harmony with the
idea of northwestward differential movements.
The very local occurrence of the phenomena in proximity to the
thrust fault at Prospect and the remarkable coincidence of the
strikes of this fault, the distinct folds in the Trenton formation,
and the folds and fractures within the contorted zones are facts
not to be lightly brushed aside by saying: “ Precisely the local
occurrence of the phenomenon which Miller emphasizes appears
to me to be out of harmony with his explanation. The cited parallel-
ism of the movements is moreover in no sense proof, since to be
sure the E. NE-W. SW, or in general E-W, direction already gov-
erned the Prepaleozoic Adirondack mass, consequently the later
movements followed only an inherited character.”* The present
writer fails to see how either the pressures within or the direction of
the Prepaleozoic mass in any way whatever argues against the idea
1 Hahn: Neues Jahrbuch, 36:8. 1913. Freely translated from the German.
REPORT OF THE DIRECTOR IQI4 143
of differential movements within the Trenton formation due to
lateral pressure at the time of the thrust faulting.
The submarine gliding hypothesis, as set forth by Hahn, may
well enough be the correct explanation of intraformational corru-
gations in certain regions but, as above shown, there are insuperable
difficulties in the way of applying this hypothesis to such phenomena
at Trenton Falls. It would seem that Hahn has fallen into a com-
mon error of making a single hypothesis or explanation altogether
too inclusive in its scope.
THE GREAT RIFT ON CHIMNEY MOUNTAIN
BY WILLIAM J. MILLER
THE MOUNTAIN AND ITS LOCATION
Chimney mountain lies 7 miles south-southeast of Indian Lake
village in the Adirondack mountains and in the northwestern por-
tion of the Thirteenth Lake quadrangle of the United States Geolog-
ical Survey. While making his headquarters at Indian Lake during
the summer of 1914, the writer’s attention was repeatedly called to
a rather remarkable feature toward the top of the mountain and
variously ascribed to “some convulsion of nature,” “ volcanic
action,” or the “ splitting open of the mountain.” This paper very
briefly gives the results of an examination of the locality, and it is
in fact not much more than an explanation of the accompanying
plates and figures.
Chimney mountain has two summits about a fourth of a mile
apart, the eastern point reaching an altitude of 2705 feet, and the
western point about 2640 feet. The Hamilton-Warren county line
passes across the mountain between these two summits. Facing the
west, the mountain side is very steep with a descent of goo feet in
a half mile.
3)
THE GREAT RIED
The phenomenon of special interest is a sreat rift with stiles
N 20° E directly across the eastern summit of the mountain (see
plate 1 and figure 3). Exact figures were not determined, but the
rift has an estimated length of 600 to 700 feet; maximum depth of
200 to 250 feet; and maximum width across ne top of 250 to 300
feet. On the eastern side of the chasm, the wall is very steep to
almost precipitous, while the greatest angle of the slope on the
western side is about 50 degrees. The highest point is the summit
of the so-called “ Chimney rock” which rises pinnaclelike on the
eastern side of the chasm (see plate 2) and some 50 or 60 feet higher
than the highest portion of the western side of the chasm directly
144 NEW YORK STATE MUSEUM
opposite. In the bottom of the rift and also at the eastern base of
the Chimney rock mass there are great accumulations of angular
blocks of rock, often 10 to 20 feet across, which have rolled down
the steep slopes since the development of the chasm.
The fact that, not many years ago, a forest fire made an almost
clean sweep of the vegetation from this portion of the mountain
causes the chasm and its immediately surrounding rock masses to
be very plainly visible.
THE ROCKS
All the exposed rocks are of Precambric age, the main mass of
the mountain consisting of fairly homogeneous, moderately gneiss-
oid, granitic syenite, with Grenville strata resting against the western
side. The rift is wholly developed within the Grenville strata, which
there have a visible thickness of about 250 feet. These rocks, which
are very distinctly stratified in layers from 6 inches to 4 or 5 feet
thick, are rusty looking biotite-quartz-feldspar gneisses, greenish-
gray pyroxene (coccolite)-feldspar gneisses, and some beds of
quartzite.
On the western side of the chasm the rocks strike N 20° E or
parallel to the rift and dip 50 degrees westward, this strike and dip
being uniform down the whole western face of the mountain. On
the eastern side of the chasm the strike and dip are quite different,
being N 40° W with greatest dip (at Chimney rock) of 20 degrees
toward the northeast.
It is important to note that in spite of such marked differences in
strike and dip, the rocks on opposite sides of the rift are of exactly
the same character in every respect, and it is certain that they were
once parts of a continuous mass.
Prominent joint-planes, mostly ERS Te ay, at right angles to
the bedding planes, are common, so that frequently large joint-
blocks loosen and slide down the steep slopes.
The exact character of the Grenville strata immediately beneath
the exposed gneisses just described is not known though, as will
be explained below, they are quite certainly relatively weaker rocks.
That they are probably either limestones or at least limestone (or
calcareous) strata interbedded with gneisses is strongly suggested
by the fact that Grenville beds very similar to those of Chimney
mountain are often directly associated with limestone in the central
and southern Adirondacks, such association having been frequently
observed by the writer in the vicinity of Indian Lake village and in
the valleys between that village and Chimney mountain. At the
W.J. Miller, photo.
Looking northward through the great rift on Chimney mountain, with
Chimney rock on the right
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View of Chimney rock as seen directly across the rift from the highest
point on the western side
REPORT OF THE DIRECTOR IQI4 145
bottom of the chasm, where one would expect to get some clew to
the character of the underlying strata, the heavy covering of rock
debris conceals everything.
CAUSE, OF: THE RIE VY
Examination of the accompanying figures will make clear the
history of the development of the great rift. The lapping of the
Grenville strata against the side of the hard, homogeneous syenite
of the mountain mass, with the weaker beds practically in contact
with the igneous rock, was decidedly favorable for undermining
(figure 1) due to removal of the weaker material by erosion or
solution, or both combined, by waters coming down from the higher
portion of the mountain during heavy rains or melting snows.
Instead of the type of undermining indicated in figure 1 there may
have been removal only of certain calcareous layers or possibly a
thorough honey-combing of the underlying weaker mass thus greatly
weakening the support of the overlying mass.
Finally the undermining proceeded far enough so that a great
block of gneiss, already practically separated by a prominent joint-
plane from the ledge of the mountain side, was suddenly pulled over
by the force of gravity (probably aided by the wedge-work of ice)
as shown in figure 2. This great block, from 600 to 700 feet long
and from 100 to 250 feet high, swung through an angle of 60 to 70
degrees with greatest subsidence toward the north, thus readily
accounting for the marked differences of strike and dip of strata
on opposite sides of the rift. It is difficult to conceive how such
an undermining process could have been carried far enough unless
we postulate relatively weaker or more soluble rock underlying the
Grenville gneisses.
That the great block fell no less than 75 to 100 years ago is
proved by the fact that trees of considerable size have grown within
the chasm, while the large accumulation of talus materials suggests
a much longer time than 100 years. On the other hand, the rift is
certainly Postglacial as indicated ‘by the utter absence of any evi-
dence of glaciation within it.
As a result of a moderate amount of weathering and the sliding
of joint-blocks down the steep slopes, the present-day conditions
were reached as shown in figure 3.
The geological principles of undermining etc. here set forth are
by no means uncommon, but the development of such a great rift
in this manner is somewhat unusual, and it appears to be quite
unique in the Adirondack region.
146 NEW YORK STATE MUSEUM
hig.
ere limestone or other saan Precambric granitic
relatively weak rock. syenite
: SCALE
Fj Grenville neisses — 600 FT.
distinctly sfratified
East-west structure sections through the western side of Chimney mountain
(looking northward)
Fig. 1 Showing essentially the condition of things not long before the
development of the great rift. The position of a prominent joint plane is
indicated in the Grenville gneisses.
Fig. 2 Showing essentially the condition of things immediately after the
development of the great rift due to breaking away of a large block from
the parent ledge of Grenville gneisses.
Fig. 3 Showing the present condition after some weathering and the ac-
cumulation of large, angular rock fragments at the bases of the steep slopes.
THE ORISKANY — PIC D’AURORE EPISODE
OF THE APPALACHIAN DEVONIC
BY JOHN M. CLARKE
Theme. In the northeastern Appalachians the Oriskany episode
was represented by a heavy deposit of shoal-water sand with the
same peculiar fauna that characterizes the sands of this period in
the central Appalachian region. This development appears to be
restricted wholly to one of the northern channels which follow close
upon the line of the River St Lawrence downthrow.
The Oriskany sedimentation in New York is now understood as
the record of a transgressing shelf sea in which the obvious move-
ment of the water was progressively west-northwest. Both in
petrology and biology this movement is clear. The shallow waters
bounded a continent which lay not far to the north, about the in-
terior sea of Appalachia, and were receiving a heavy landwash
from subsiding shores; tides and the undertow washed the fine
muds far out leaving behind in the shoal waters a clean quartz sand.
In New York these sands carry what is historically the typical
fauna of the formation, for it was the first to become known and is
still to be regarded as the characteristic biota of the “ Oriskany.”
This assembly was largely made up of heavy shells, both of brachio-
pods and gastropods, and it has been a frequently expressed con-
ception that such ponderous shells as these were a direct response
to the demand for more secure protection in the play and pounding
of the waves along the strand. There is, however, a well-known
and so-called “ calcareous Oriskany ” in southeastern New York, a
region where a larger and much more variant fauna existed and
where the sediments are indicative of deeper water because of the
presence of lime. These deeper sediments carry a very large silica
and clay content, and the condition of the silica is not that of
quartz sand nor can it yet be safely regarded as the fine silicious
outwash from the shore. The petrology of this silica content has
yet to be fully deciphered. Its chert masses and the irregular dis-
tribution of the silica matrix indicate secondary change and quite
possibly an obscure benthonic fauna not yet known. The very
clear distinction between the fauna of the sands and of the lime-
stones is recognized, and it is evident that, in these New York oc-
currences at least, the heavy species which locally abound in the
148 NEW YORK STATE MUSEUM
sands are rare in the limestones, and when they do occur are quite
likely to be of smaller size. The inference from these conditions
has been a natural and easy one and is to this effect: that the sand
fauna represents the shoreward movement of the fauna of the
period and is composed of well-adjusted representatives and sur-
vivors of the deeper water. This is a conclusion which is quite
reasonably applicable to such conditions, for we must often interpret
these near-shore faunas in terms of migration from the outer sea.
In actual succession the sand beds of the Oriskany are a later
term than the lime beds of Hudson, Glenerie, Highland Mills, Otis-
ville etc., but this fact does not affect the fauna as such; a re-
adjusted element out of the more prolific deeper water reservoir.
Turning to the expression of this Devonic episode in the north-
eastern Appalachians, we find a better evidence for the inferences
above intimated, for there it is obvious, in the first place, that there
is no real “facies” relation between the sandstone fauna and its
environment, and it becomes perfectly clear that the sand species
of New York must be regarded as only happy readjustments which
traveled into shoal waters from the deeper biota, because this asso-
ciation has in full exemplification all the elements of the fauna to-
gether, brachiopods and gastropods with their full weight of shell,
in the lower or Oriskany horizon of the Grande Gréve limestones.
The Grande Greve limestones constitute a series which is faunally
comprehensive, for its upper beds carry clear indications of a later
than Oriskany fauna, while its lower beds express the Oriskany
element; and in its petrology it is a mass of deposits gradually in-
creasing in purity of lime from the bottom up, while the impurity
of the lower layers is not silica in the form of sand but a clay-
silica matrix. In the higher beds the silica becomes much more
obvious and often is segregated into horizontal chert masses, and
even where the limestone appears to be pure there is often a large
residuum of silica which in spots is practically composed of masses
of silicious sponge spicules.
The expression of the Oriskany sedimentation episode in the
Grande Gréve series of northeastern Gaspé is highly typical and
apparently perfectly normal. Here exist, for example, heavy
Rhynchonellas, Hipparionyx, Rhipidomella, Chonetes, Spirifer,
Rensselaeria and Diaphorostoma, as in the sandy Oriskany of New
York, with no diminution of size or weight but in a highly cal-
careous matrix and in association with species which farther west-
ward represent the earlier facies of the Oriskany in New York.
REPORT OF THE DIRECTOR IQI4 149
In this northern Gaspé region the shoal-water sand and the shoal-
water fauna as such are apparently quite absent from the series.
I have recently had occasion to describe the Pic d’Aurore section.’
The Pic d’Aurore is the high, transected vertical mountain face
which overhangs Malbay and faces the north shore of Percé on the
Gaspé front. The cliff section here is a reasonably long one, ex-
tending a distance of about 3 to 4 miles from Cape Barré at Percé
to Cannes-des-Roches and thence on to Corner-of-the-Beach. The
section from Cape Barré, which is at the Percé end and therefore
at the east, three-fourths of the distance to Cannes-des-Roches, is
composed wholly of the much contorted pre-Bonaventure rocks,
and in the Pic d’Aurore, where the section reaches its maximum
height, the rocks of the Lower Devonic are best exposed.
Previous descriptions have made it obvious that the Percé lime-
stone, which constitutes the Percé rock and a part of the sea cliff
of Pic d’Aurore, is, on the basis of community of species, con-
tinuous with the Grande Gréve limestone, but it has not been
assumed at any time that the Percé limestone was to be closely
paralleled with the Oriskany division of the Grande Gréve lime-
Gane bie sacesoiothe Pie d Aurore and of the entire line ofthe
cliff wall, known in the community as “ Les Murailles,” is brilliantly
colored, and in the Pic d’Aurore itself much of this color, in the
lower and vertical beds, is due to a washing down of color from the
horizontal red Bonaventure beds, which form a cap to the summit.
The inaccessibility of the cliff face, the masking of essential by
secondary structures and the diffused coloration of the section easily
confuse the observer so that the interpretation of the succession is
not without difficulties. I bring it to notice in this connection be-
cause of its demonstration of the fact that in this part of Gaspé
the shoal sedimentation of the Oriskany episode was actually highly
developed. Here is a fairly close fold of the beds lying beneath
the Percé limestone and the order of succession will be intelligible
from the diagram facing page 152.
The “ Percé limestones” are here underlain by rather thick series
of white or greenish-gray sandstones which are essentially devoid
of fossils though carrying traces of something like a Cladopora.
They are for the most part thin bedded and are not of a sort to
promise much in the way of fossil content, though in their lower
part, on the west flank of the syncline, they have produced
1 Geological Society of America, Philadelphia meeting 1014.
150 NEW YORK STATE MUSEUM
Spirifer murchisoni and Rhipidomella museme
losa. In the midst of these folded sandstones, however, on the
east flank of the anticline, les a darker sandstone band in which
the grains are notably coarse, in places actually pebbles, and here,
in bad preservation, occurs the typical sand fauna of the New York
Oriskany; that is to say, Rensselaeria ovoides, Lege
taena ventticosa,:. Spiriter sarenoemwss. icine
coelia flabellites, Hippario ay tp0 1a eee
phorostoma ventricosa and a large Pterinea; no other
fossils have been observed and none at all that would be regarded as
tying this fauna and its formation to the deeper waters or the
deeper water fauna.
The Barré limestone at the eastern end of the section is known
to contain the trilobite Dicranurus, and this alone is evidence of its
very earliest Devonic age, and the horizon is thus, rightly I think,
construed as the base of the entire Devonic section. The contact
between this and the Percé limestone on this cliff section is a fault,
as is very clearly shown. It is probable that the Barré limestone
is a term lying beneath the limestones of the Pic d’Aurore fold, in
view of the recognizable difference in petrology and the fauna. The
Pic d’Aurore series is the term now used for this succession of
predominant sand sedimentation with intermingled limestone beds,
and it may be regarded as extending from the base of the Perce
limestone down to the’ contact line between the sandstones and top
of the Barré limestone.
The contact of the Devonic with the earlier beds is an uncon-
formity at the west of this section and both Siluric and Ordovicic
strata are exposed at the base of the cliff near the mouth of the
couleé which runs down at this point from the face of the Grand
Coupé in Percé mountain. On the other side of this couleé the
cliff is composed of further development of the corrugated Siluric
beds above with Ordovicic beds beneath. From this point the
section on to Cannes-des-Roches or the northwest end of the cliffs
is represented as composed entirely of the green and mottled marls,
red sandstones and dark shales of the Bonaventure conglomerate,
all of which have obviously been overturned from the Table-a-
rolante and which form only a thin veneer overlying the seaward
edges of the Siluric-Ordovicic beds.
REPORT OF THE DIRECTOR IQT4 Pat
The “Oriskany” band (dark lined) in the Pic-d’Aurore formation
This layer is a band of only 2 or 3 feet in thickness, and with
the white sandstones above and below, the total thickness of the
sand deposition is 100 feet or more. Under the sands in the heart
of the anticline comes a blue-gray limestone becoming brown and
dolouivc: Leptaecna rhomboidalis, a large Palaeoneilo
and a coarse meshed Dictyonema have been found, but the beds are
specially characterized by the abundance of Haliserites, a Fucus
highly characteristic of the early Devonic of western Europe but
essentially absent elsewhere from the Appalachian record. Below
this horizon are red-yellow platten-limestones with a large element
of sand, and these are visible in the section only on the western limb
of the syncline. In these beds has been found a very large Homa-
lonotus having a body width of 3 inches, and a large Diaphorostoma.
After some 40 feet of these beds follow below 75 feet more of much
distorted and corrugated green-gray thin sandstones which bend
upward to an almost vertical position.
The succession of this entire series shows a marked diversity on
the two flanks of the folds, the true Oriskany fauna with its dark
sandstone band at the east not appearing at the west, and the lime-
stones beneath, constituting the part of the decapitated fold, are
identifiable on the uprise at the west only as interbedded with the
sandstones. This change is probably somewhat exaggerated in the
sketch here given, but it is evident that the close folding has squeezed
out these limestones in some measure, and, further, that the sand-
stones which make the lowest term at the west were not caught in
the edges of the fold and are thus not represented on the eastern
slope.
152 NEW YORK STATE MUSEUM
Explanation of Pic d’Aurore section. This is the cliff section ex-
tending from southeast to northwest and facing the Mal-Baie. The
attempt has been made to give the strata approximately their
natural coloration in the morning sun, though actually the red color
of the summit peak is spread downward by the leaching of the
rains over the surface of the less brilliantly tinted strata. The
height of the Pic d’Aurore is about 800 feet. A part of the village
in the north bay of Percé is seen beyond Barré cape. The section
cuts the Appalachian folds of the Precarboniferous Paleozoic some-
what obliquely but is almost at right angles to the section on the
gulf front at Percé from Cape Barré south.
The mountain in the background is the plateau or relict-mountain,
the Table-a-rolante, to whose type of structure reference is made
again in the following paper. This relict-mountain is composed of
red Bonaventure or post-mid-Devonic-Carbonic and sands and con-
glomerates lying in low waves dipping toward the north, and its
beds rest on the eroded folds of the Paleozoics. A moiety of these
horizontal Bonaventure beds makes the summit of the Pic d’Aurore
where they lie on a truncated anticline of the Devonic series.
Bonaventure conglomerate. All the northwestern end of this
section is constituted of this formation and the strata here slope
evenly to the water so that the observer from the present point of
view looks against the up-surface of one bed or of closely successive
beds. This mass of the Bonaventure has obviously fallen down and
over from the horizontal plateau mass above, from which it has
been rifted. Sections across this mass at right angles to the shore
show it to be a mere veneer leaning against the Siluric-Ordovicic
beds. The angle of attitude in these Bonaventure marls and sand-
stones lessens toward the west, and at the end of the section at
Cannes-des-Roches the beds lie again in a horizontal position. The
rocks are mostly gray-green and mottled sandy marls, with some
sharply outlined beds of red sandstone and conglomerate layers,
and the edge of one of these, where the stratum has been broken
off and slipped into the sea, is shown at the right. There are also
some patchy layers of dark shale.
Next follows in order of succession downward the Percé lime-
stone, which here makes the Trois Soeurs or the three cliffs at left
of the Pic d’Aurore, and whose closely infolded remnant is seen
at the right on the flank of the Pic.
Below is the Pic d’Aurore series in characteristic close folds ; first,
the white sandstone showing in the east flank the dark band with
agile. ee ee ei Sie oe act ar nit Ot Sate
SILURIAN ORDOVICIAN
eve’.
eo ie GE
ae
1
q
d
a
S)
% Ke
% +
a7
_ Ri
ray
StF
rt
wa
a tea |
| ao
i. b= |
1 + a
{ %
| -t
\ . 3 4
| | {
in, Case
Nine
} Mie ;
| oat
q , ‘. = ,
} 7 eh
| eae
y k ¢
Pp / ‘ "
¥ } if
5
—
' Explanation of Pic d’Aurore section. {Wis is the cliff section &
' tending from southeast t northwest and facing the Mal-Baie, The}
attempt has been mae te gee the strata approximately their ”
natural coloration in the siting eps though actually the red color
of the summit peak is spreat howeetd by the ee of the)
rains over the surface of ths Wax y Plante The?
height of the Pic d’Aurore is aber par |
‘in the north bay of Percé is seen twyemt Bae
cuts the Appalachian folds of the Precarbonifer:
what obliquely but is almost at right angles ‘to the
gulf front at Percé from Cape Barré south. 4
The mountain in the sd aspacie is the plateau § or relict-me 0
again in the cliowige paper. This avenue is onip:
red Bonaventure or post-mid-Devonic-Carbonic and sands a
glomerates lying in low waves dipping toward the north, a 1
beds rest on the eroded folds of the Paleazoics. A moiety of
Horizontal Bonaventure beds mukew the simmit of the Pic d’Auro
where: they lie on a trimcated anticline of the Devonic series, 3
Bowwenture conglomerate, AW the sorthwestern end of this |
section is constituted of this formation and the strata here slope |
evenly te the water sq that the observer frorm the present point of 7
view looks sgninet the upsurface of one bed or of closely successive —
beds. Tliis stax of the Bonaventure has obviously fallen down and
over from the horizontal plateau mass above, from which it h
been rifted. Sgotions across this mass-at right angles to the sk ore |
show it to be a mere yeneer leaning against the Siluri¢-Or =
beds. The angle of attitude in these Bonaventure mars anit
stones lessens toward the west, and at the end of te
Cannes-des-Roches the beds lie again in # hee eh
rocks are mostly gray-green and mptilel &
earely outlined beds of ‘- : aed
Of and eisied into the paneer whos ee
some patchy layers of dark shate,
Next follows in order of
stone, which here makes ti
2 fer nthe nk of e
| 1S ngoe'slahana ata
ee ee
AURORE
pet SS —— — 2 SEs
e are 2 az PIC , D’AURORE ~ sag
THE UNIVERSITY OF THE STATE OF NEW YORK
_ Reports 2, 8-12 may also be obtained bound in cloth at 25c each in addition to the price
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1 Zoology Use 60 Zoology 119 Economic Geology
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50 Archeology 1og Entomology 168 Geology
51 Zoology 110 ie 169 i
52 Paleontology rrr Geology 170 x
53 Entomology I12 oongune Geology ve et
4 Botan II tcheolo ike
Be Areheelane te Geology = 173 Director’s report for 1913
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59 Entomology 118 Geology 177 Director’s report for 1914
MUSEUM PUBLICATIONS
Bulletins are also found with the annual reports of the museum as follows:
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12-15 48,v.1 79 By Vie te pt 2 PrO—2te Om, Vent I54 64, Vv. 2
roxy BOgavet 80 eS Du La aie 61, V. 2 I55 Osu 2
18,19 reve Tt 81,82 58, Vv. 3 I23 GE Vor 156 OR) we 2
20-25 52, Ve x 83,84 Roe ved 124 61, Vv. 2 157 sia Nie
26-31 Rah TT: 85 58, v. 2 I25 62,Vv.3 158 Os Veal
32-34 Enea: 80 Raa 126-28 62,V.1 159 O5. Vee
35,36 54, Vv. 2 87-89 58, Vv. 4 129 62y-Ve2 160 Obs Ved
37-44 ° 54,V.3 go 58, v.3 I30 62, V.3 IOI O5..vn 2
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57 56, Vv. 3 95,96 oie Nits ike 136 63, Vane 168-70 66, v. I
58 56.) Ve 5 97 58, Vv. 5 137 63,V.1
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70 GRAS alte JOR Ey Bia OOsWis 153 G4, ve 2 TAR ene 65, Vv. 4
78 B7aave 2 118 60, V. I
The figures at the beginning of each entry in the following list indicate its number as a
museum bulletin.
Geology and Paleontology. 14 Kemp, J. F. Geology of Moriah and West-
port Townships, Essex Co., N. Y., with notes on the iron mines. 38p.
il. 7pl. 2 maps. Sept. 1895. Free.
19 Merrill, F. J. H. Guide to the Study of the Geological Collections of
the New York State Museum. 164p. 119pl. map. Nov. 1898. Out of print.
21 Kemp, J. F. Geology of the Lake Placid Region. 24p. rpl. map. Sept.
1898. Free.
34 Cumings, E. R. Lower Silurian System of Eastern Montgomery County;
Prosser, C. S. Notes on the Stratigraphy of Mohawk Valley and Sara-
toga County, N.Y. 74p.14pl.map. May 1900. Not available.
39 Clarke, J. M.; Simpson, G. B. & Loomis, F. B. Paleontologic Papers 1,
72D iW TOpL Mr Oeh L900. 15C.
Contents: Clarke, J. M. A Remarkable Occurrence of Orthoceras in the Oneonta Beds of
the Chenango Valley, N. Y
—— Paropsonema cryptophya; a Peculiar Echinoderm from the Intumescens-zone
(Portage Beds) of Western New York.
—— Dictyonine Hexactinellid Sponges from the Upper Devonic of New York.
—— The Water Biscuit of Squaw Island, Canandaigua Lake,
Simpson, G. B. Preliminary Descriptions of New Genera of Paleozoic Rugose Corals.
Loomis, F. B. Siluric Fungi from Western New York.
42 Ruedemann, Rudolf. Hudson River Beds near Albany and their Taxo-
nomic Equivalents. 116p. 2pl. map. Apr. Ig01. 25¢c.
45 Grabau, A. W. Geology and Paleontology of Niagara Falls and Vicinity.
250p eatepl. map. Apr. igor.’ 65¢; clotiz, 906.
48 Woodworth, J. B. Pleistocene Geology of Nassau County and Borough
of Queens. 58p. il. 8pl. map. Dec. 1901. Not available.
49 Ruedemann, Rudolf; Clarke, J. M. & Wood, Elvira. Paleontologic
Papers 2. 240p. 13pl. Dec. r901. Out of print.
Contents: Ruedemann, Rudolf. Trenton Conglomerate of Rysedorph Hill.
Clarke, J. M. Limestones of Central and Western New York Interbedded with Bitumi-
nous Shales of the Marcellus Stage.
Wood, Ele Marcellus Limestones of Lancaster, Erie Co., N. Y.
Clarke, J. M. New Agelacrinites.
Value of Amnigenia as an Indicator of "Fresh- water Deposits during the Devonic of
New York, Ireland and the Rhineland.
52 Clarke, J. M. Report of the State Baletnieinoe es TOOT. 28opcsk rep.
map, tab.’ July*1goe) ~40¢e,
THE UNIVERSITY OF THE STATE OF NEW YORK
56 Merrill, F. J. H. Description of the State Geologic Map of rgor. 4ap.
2 maps, tab. Nov. 1902. Free.
63 Clarke, J. M. & Luther, D. D. Stratigraphy of Cananadigua and Naples
Quadrangles. 78p. map. June 1904. 25¢.
65 Clarke, J. M. Catalogue of Type Specimens of Paleozoic Fossils in the
New York State Museum. 848p. May 1903. Not available.
69 Report of the State Paleontologist 1902. 464p. 52pl.7 maps. Nov.
TOOZ. ia cloue: :
77 Cushing, H. P. Geology of the Vicinity of Little Falls, Herkimer Co.
98p. 1. a5pl. 2amaps:) Jan n9o5.. oc:
80 Clarke, J. M. Report of the State Paleontologist 1903. 396p. 2opl.
2 maps. Feb. 1905. 85c, cloth.
81 Clarke, J. M. & Luther, D. D. Watkins and Elmira Quadrangles. 32p.
igakehoy WWlavins TelSligw ASCs
82 Geologic Map of the Tully Quadrangle. 4op.map. Apr.1905. 20C¢.
83 Woodworth, J. B. Pleistocene Geology of the Mooers Quadrangle. 62p.
25pl. map. june 190s, 7 25e.
Ancient Water Levels of the Champlain and Hudson Valleys. 206p.
io Triple noemaps..n)dlyan oon: ee
90 Ruedemann, Rudolf. Cephalopoda of Beekmantown and Chazy For-
mations of Champlain Basin. 224p. il. 38pl. May 1906. 75¢c, cloth.
92 Grabau, A. W. Guide to the Geology and Paleontology of the Schoharie
Region 214ip.il: 2oplaimaps Apr 1906. 4 75¢,clor:
95 Cushing, H. P. Geology of the Northern Adirondack Region. 188p.
To ple Smaps. Se pts 1Oa5. uN sOC:
96 Ogilvie, I. H. Geology of the Paradox Lake Quadrangle. jap. il. r7pl.
map. Dec. 1905. Not available.
99 Luther, D. D. Geology of the Buffalo Quadrangle. 32p. map. May
LOCO. ZOC:
roa Geology of the Penn Yan-Hammondsport Quadrangles. 28p.
map. July 1906. Out of print.
106 Fairchild, H. L. Glacial Waters in the Erie Basin. 88p. r4pl. 9 maps.
Feb. 1907. Out of print.
1o7 Woodworth, J. B.; MartnagelC..A Whitlock, EU Pe) Hudson G. a:
Clarke, J. M.; White, David & Berkey, C. P. Geological Papers. 388p.
54pl. map. May 1907. goc, cloth.
Contents: Woodworth, J. B. Postglacial Faults of Eastern New York.
Hartnagel, C. A. Stratigraphic Relations of the Oneida Conglomerate.
Upper Siluric and Lower Devonic Formations of the Skunnemunk Mountain Region.
Whitlock, H. P. Minerals from Lyon Mountain, Clinton Co.
Hudson, G. H. On Some Pelmatozoa from the Chazy Limestone of New York.
Clarke, J. M. Some New Devonic Fossils.
An Interesting Style of Sand-filled Vein.
—— Eurypterus Shales of the Shawangunk Mountains in Eastern New York.
White, David. A Remarkable Fossil Tree Trunk from the Middle Devonic of New York.
Beye C. P. Structural and Stratigraphic Features of the Basal Gneisses of the High-
ands.
rrr Fairchild, HL. Drumlmsiot New Work joopsezople Lo naps. ) auly
1907. Out of print.
114 Hartnagel, C. A. Geologic Map of the Rochester and Ontario Beach
Quadrangles. 36p. map. Aug. 1907. Not available.
115 Cushing, H. P. Geology of the Long Lake Quadrangle. 88p. 2opl.
map. Sept. 1907. Out of print.
118 Clarke, J. M. & Luther, D. D. Geologic Maps and Descriptions of the
Portage and Nunda Quadrangles including a map of Letchworth Park.
50p. Lopl. 4 maps. Jani meoca asc:
126 Miller, W. J. Geology of the Remsen Quadrangle. 54p. il. rrpl. map.
Jan. 1oso7)) 256
127 Fairchild, H. L. Glacial Waters in Central New York. 64p. 27pl. 15
maps. Mar. 1909. Out of print.
128 Luther, D. D. Geology of the Geneva-Ovid Quadrangles. 44p. map.
Apr. 1909. Not available.
135 Miller, W. J. Geology of the Port Leyden Quadrangle, Lewis County,
N.Y. Gop:alaipl imap, ejaaeaamoneece:
MUSEUM PUBLICATIONS
137 Luther, D. D. Geology of the Auburn-Genoa Quadrangles. 36p. map.
Mar. 1910. 20C.
138 Kemp, J. F. & Ruedemann, Rudolf. Geology of the Elizabethtown
and Port Henry Quadrangles. 176p. il. 2opl.3 maps. Apr. 1g10. Not
available.
145 Cushing, H. P.; Fairchild, H. L.; Ruedemann, Rudolf & Smyth, C. H.
Geology of the Thousand Islands Region. t1g4p. il. 62pl.6 maps. Dec.
t910. Not available.
146 Berkey, C. P. Geologic Features and Problems of the New York City
(Catskill) Aqueduct. 286p. il. 38pl. maps. Feb. 1911. 75c; cloth, $1.
148 Gordon, C. E. Geology of the Poughkeepsie Quadrangle. 122p. il.
26pl.-mapis Apr. 1ori=.°30c.
152 Luther, D. D. Geology of the Honeoye-Wayland Quadrangles. 3op.
map: Oct. 191i. (20c.
153 Miller, William J. Geology of the Broadalbin Quadrangle, Fulton-
Saratoga Counties, New York. 66p.. il. 8pl. map. Dec. 1911. Not
available.
154 Stoller, James H. Glacial Geology of the Schenectady Quadrangle. 44p.
gpl. map. Dec.1911. Not available.
159 Kemp, James F. The Mineral Springs of Saratoga. 8o0p.il. 3pl Apr.
1912. Not avaziable.
160 Fairchild, H. L. Glacial Waters in the Black and Mohawk Valleys. 48p.
il. 8pl.14 maps. May 1912. 50c.
162 Ruedemann, Rudolf. The Lower Siluric Shales of the Mohawk Valley.
T52p. tberspl, Aug. 1912: 35c.
168 Miller, William J. Geological History of New York State. I30p. gpl.
TOrmMaps... Wee: 1OLZ.- AOC:
169 Cushing, H. P. & Ruedemann, Rudolf. Geology of Saratoga Springs and
Vicinity. 178p.il.20 pl. map. Feb. 1914. 4oc.
170 Miller, William J. Geology of the North Creek Quadrangle. gop. il. r4pl.
Feb. 1914. Not available.
171 Hopkins, T.C. The Geology of the Syracuse Quadrangle. 8op. il. 2opl.
map. July 1914. Not avazlable.
172 Luther, D. D. Geology of the Attica and Depew Quadrangles. 32p. map.
August 1914. Not available.
Miller, William J. The Geology of the Lake Pleasant Quadrangle. Im press.
Stoller, James H. Glacial Geology of the Saratoga Quadrangle. In press.
Miller, William J. Geology of the Blue Mountain Quadrangle. Prepared.
Martin, James C. & Chadwick, George H. Geology of the Canton Quad-
rangle. Prepared.
Luther, D.D. Geology of the Phelps Quadrangle. In preparation.
Whitnall, H. O. Geology of the Morrisville Quadrangle. Prepared.
Hudson, G. H. Geology of Valcour Island. In preparation.
Economic Geology. 3 Smock, J. C. Building Stone in the State of New
York. 154p. Mar. 1888. Out of print.
First Report on the Iron Mines and Iron Ore Districts in the State
of New York. 78p. map. June 1889. Out of print.
Building Stone in New York. 210p. map, tab. Sept. 1890. Not
avatlable.
1r Merrill, F. J. H. Salt and Gypsum Industries of New York. og 4p. r2pl.
2 maps, 11 tab. Apr. 1893. Not available.
12 Ries, Heinrich. Clay Industriesof New York. 174p.il. 1pl.map. Mar.
FOg5. = 406:
15 Merrill, F. J. H. Mineral Resources of New York. 240p. 2 maps.
Sept. 1895. [soc]
17 Road Materials and Road Building in New York. 5z2p. r4pl.
2 maps. Oct. 1897. Not available.
30 Orton, Edward. Petroleum and Natural Gas in New York. 136p. il.
3 maps. Nov. 1899. 15¢c.
35 Ries, Heinrich. Clays of New York; their Properties and Uses. 456p.
140opl. map. June 1900. Out of print.
Lime and Cement Industries of New York; Eckel, E. C. Chapters
on the Cement Industry. 332p. 1o1pl. 2 maps. Dec. rgor. 85, cioth.
Io
44
THE UNIVERSITY OF THE STATE OF NEW YORK
61 Dickinson, H. T. Quarries of Bluestone and Other Sandstones in New
L..York. sr14p. 18pl. 2 maps. Mar. 1903. 35¢c.
85 Rafter, G. W. Hydrology of New York State. go2p. il. 44pl. 5 maps.
rx May 1905. $1.50, cloth.
93 Newland, D. H. Mining and Quarry Industry of New York. 78p.
July 1905. Out of print.
too McCourt, W. E. Fire Tests of Some New York Building Stones. 4op.
26pl. Feb. 1906. 15c.
1o2 Newland, D. H. Mining and Quarry Industry of New York 1905.
162p. June 1906. 25¢.
112 Mining and Quarry Industry of New York 1906. 82p. July
1907. Out of “print.
119 & Kemp, J. F. Geology of the Adirondack Magnetic Iron Ores
;- With a Report on the Minev ille-Port Henry Mine Group. 184p. ra4pl.
8 maps. Apr. 1908. 35¢C.
120 Newland, D. H Mining and Quarry Industry of New York 1907. 8ap.
July 1908. Out of print.
123 & Hartnagel, C. A. Iron Ores of the Clinton Formation in New
York State. 6p. il. 14pl. 3 maps. Nov. 1908. 25C¢c.
132 Newland, D. H. Mining and Quarry Industry of New York 1908. 98p.
July 1909. 15¢.
142 Mining and Quarry Industry of New York for1go9. 98p. Aug.
tg10o. Not available.
143 Gypsum Deposits of New York. 94p. 2opl. 4maps. Oct.1910 Not
available.
I51 Mining and Quarry Industry of New York igio. 82p. June1g11. Not
available.
161 Mining and Quarry Industry of New York 1g11I. 114p. July 1912. 20¢.
166 Mining and Quarry Industry of New York 1912. 114p. August 1913.
Not avazlable.
174 Mining and Quarry Industry of New York 1913. 111 p. Dec. 1914.
20¢.
Mining and Quarry Industry of New York 1914. In press.
The Quarry Materials of New York. In press.
Mineralogy. 4 Nason,F.L. Some New York Minerals and Their Localities.
22p. ipl. Aug. 1888. Not available.
58 Whitlock, H. P. Guide to the Mineralogic Collections of the New York
State Museum. r15op. il. 39pl. 11 models. Sept. 1902. 4oc.
70 New York Mineral Localities. tiop. Oct. 1903. 200.
98 Contributions from the Mineralogic Laboratory. 38p. 7pl. Dec.
1905. Out of print.
Zoology. 1 Marshall, W. B. Preliminary List of New York Unionidae.
2op. Mar. 1892. Not avazlable.
Beaks of Unionidae Inhabiting the Vicinity of Albany, N. Y. 3op.
1pl. Aug. 189c. Free.
29 Miller, Gis. jr. Preliminary List of New York Mammals. 124p. Oct.
1899. Not available.
33am M.S: Check List of New York Birds. 224p. Apr. 1Igoo. 25¢.
38 Miller, G. S., jr. Key to the Land Mammals of Northeastern North
America. 106p. Oct. 1900. Out of print.
40 Simpson, G. B. Anatomy and Physiology of Polygyra albolabris and
Limax maximus and Embryology of Limax maximus. 82p. 28pl. Oct.
1001, 256.
43 Kellogs. J. L. Clam and Scallop Industries of New York. 36p. 2pl.
map. “Apr. tgor1. Not available.
51 Eckel, E. C. & Paulmier, F.C. Catalogue of Reptiles and Batrachians
of New York. 64p. il. rpl. Apr. 1902. “Out of print.
Eckel, E.C. Serpents of Northeastern United States.
Paulmier, F.C. Lizards, Tortoises and Batrachians of New York.
9
"Sige T. H. Catalogue of the Fishes of New York. 784p. Feb. 1903.
1, cloth.
a
MUSEUM PUBLICATIONS
71 Kellogg, J. L. Feeding Habits and Growth of Venus mercenaria. 3op.
4pl. Sept. 1903. Free.
88 ree Elizabeth J. Check List of the Mollusca of New York. 116p.
May 1905. 20¢.
91 Paulmier, F. C. Higher Crustacea of New York City. 78p. il. June
20C.
130 > Shufeldt, R. W. Osteology of Birds. 382p.il. 26pl. May 1909. §5oc.
Entomology. 5 Lintner, J. A. White Grub of the May Beetle. 34p. il.
ov. 1888. Not available.
6 Cut-worms. 38p. il. Nov. 1888. Free.
13 San José Scale and Some Destructive Insects of New York State.
54p. 7pl. Apr. 1895. 15¢.
20 Felt, E. P. Elm Leaf Beetle in New York State. 46p. il. spl. June
1898. Free:
See 57.
23
14th Report of the State Entomologist 1898. 15o0p. il. gpl. Dec.
1898. Not available.
Memorial of the Life and Entomologic Work of J. A. Lintner Ph.D.
State Entomologist 1874-98; Index to Entomologist’s Reports 1-13. 316p.
Folk.,Oct: BSo9. ~-3.5c.
Supplement to 14th report of the State Entomologist.
26
“Collection, Preservation and Distribution of New York Insects.
36p. il. Apr. 1899. Out of print.
Shade Tree Pests in New York State. 26p. il. 5pl. May 1899.
27
Free.
31
36
15th Report of the State Entomologist 1899. 3128p. June rIgoo.
Not available.
16th Report of the State Entomologist 1900. 1318p. 16pl. Mar,
tgo1. Not available.
Catalogue of Some of the More Important Injurious and Beneficial
Insects of New York State. 54p. il. Sept. 1900. Not available.
Scale Insects of Importance and a List of the Species in New York
State: “/o4p.il 15pl. June oor. 25 ¢.
47 Needham, J. G. & Betten, Cornelius. Macon Insects in the Adiron-
dacks. 234p. il. 36pl. Sept. rgo01.
53 Felt, E. P. 17th Report of the State PAjemolveiat TQOT.. - 232p. il. op
Aug. 1902. Out of print.
57 Elm Leaf Beetle in New York State. 46p. il. 8pl. Aug. 1902.
Out of print.
This is a revision of Bulletin 20 containing the more essential facts observed since that
Was prepared.
46
59 Grapevine Root Worm. jop. 6pl. Dec. 1902. Not available.
See 72.
64 18th Report of the State Entomologist 1902. s110op. 6pl. May
1903. Not available.
68 Needham, J. G. & others. Aquatic Insects in New York. 322p. 5apl.
Aug. 1903. 8oc, cloth.
72 Felt, E. P. Grapevine Root Worm. 58p. 13pl. Nov. 1903. 200.
This is a revision of Bulletin 59 containing the more essential facts observed since that
was prepared.
74 - & Joutel, L. H. Monograph of the Genus Saperda. 88p. r4pl.
June 1904. 25¢.
76 Felt, E. P. soth Report of the State Entomologist 1903. 1450p. 4pl.
1904; 15e:
Mosquitos or Culicidae of New York. 164p. il. 57pl. tab. Oct.
79
1904. 40C.
86 Needham, J. G. & others. May Flies and Midges of New York. 352p.
il. 37pl. June 1905. Out of print.
97 Felt, E. P. 20th Report of the State Entomologist 1904. 246p. il. rgpl.
Nov. 1905. 40Cc
103
Gipsy and Brown Tail Moths. 44p. topl. July 1906. 1I5¢
THE UNIVERSITY OF THE STATE OF NEW YORK
104 21st Report of the State Entomologist 1905. 144p. 1opl. Aug.
1906. Not available.
109 Tussock Moth and Elm Leaf Beetle. 34p. 8pl. Mar. 1907. Not
available.
IIo 22d Report of the State Entomologist 1906. r52p. 3pl. June
EjO7. 256.
124 23d Report of the State Entomologist 1907. 542p. il. 44pl. Oct.
1908. 75C. :
129 Control of Household Insects. 48p.il. May 1909. Out of print.
134 24th Report of the State Entomologist 1908. 208p. il. 17pl.
Sept. 1909. 35¢.
136 Control of Flies and Other Household Insects. 56p. il. Feb.
EQIG! VA5FE
This is a revision of Bulletin 129 containing the more essential facts observed since
that was prepared.
141 Felt, E. P. 25th Report of the State Entomologist 1909. 178p. il. 22pl.
July 1910. Not available.
147 26th Report of the State Entomologist 1910. 182p. il. 35pl. Mar.
A gece orth Report of the State Entomologist I911. 198p. il. 27pl. Jan.
teat ‘Ein Leaf Beetle and White-Marked Tussock Moth. 35p. 8pl. Jan.
Hee “28th Report of the State Entomologist 1912. 266p. 14pl. July 1913.
Not available.
175 29th Report of the State Entomologist 1913. 258 p. 16 pl. April
I9QI5. 465¢.
ae 30th Report of the State Entomologist 1914. In press.
Needham, J. G. Monograph on Stone Flies. In preparation.
Botany. 2 Peck, C. H. Contributions to the Botany of the State of New
York. yz2p. 2pl. May 1887. Out of print.
Boleti of the United States. g98p. Sept. 1889. Out of print.
25 Report of the State Botanist 1898. 76p. spl. Oct. 1899. Out of
rint.
re Plants of North Elba. 206p. map. June 1899. 200.
54 —— Report of the State Botanist 1901. 58p. 7pl. Nov. 1902. 4oc.
67 —— Report of the State Botanist 1902. 1196p. 5pl. May 1903. Soc.
75 —— Report of the State Botanist 1903. 7op. 4pl. 1904. 4oc.
904 —— Report of the State Botanist 1904. 6op.i1opl. July 1905. 4o0c.
105 —— Report of the State Botanist 1905. 108p.12pl. Aug.1906. Soc.
116 Report of the State Botanist 1906. 120p. 6pl. July 1907. 35¢c.
I22 Report of the State Botanist 1907. 178p. 5pl. Aug. 1908. 4oc.
I31 Report of the State Botanist 1908. 202p. 4pl. July 1909. 4oc.
Report of the State Botanist 1910. troop. spl. May 1911. 3oc.
Report of the State Botanist 1911. 140p. gpl. Mar. 1912. 365c.
Report of the State Botanist 1912. 138p. 4pl. Sept. 1913. 30c.
176 —— Report of the State Botanist 1913. 78p. 17pl. June 1915. 20¢.
Report of the State Botanist 1914. In press.
Archeology. 16 Beauchamp, W. M. Aboriginal Chipped Stone Implements
of New York. 86p. 23pl. Oct. 1897. Not available.
Polished Stone Articles Used by the New York Aborigines. 1o4p.
acpl:. Ney:. sGo75,, S5e:
Earthenware of the New York Aborigines. 78p. 33pl. Oct. 1898.
139 —— Report of the State Botanist 1909. 116p.10opl. Maystgio. 45¢c.
18
22
25¢
32 Aboriginal Occupation of New York. t1go0p. 16pl. 2 maps. Mar.
1900. 30c:
Wampum and Shell Articles Used by New York Indians. 166p.
28pl. Mar. 1901. Out of print.
Horn and Bone Implements cf the New York Indians. 112p. 43pl.
Mar. 1902. Out of print.
50
MUSEUM PUBLICATIONS
Metallic _ Implements of the New York Indians. g4p. 38pl. June
1902. Not available.
Metallic Ornaments of the New York Indians. t122p. 37pl. Dec.
1903. Not available.
History of the New York Iroquois. 340p. 17pl. map. Feb. 1905.
Not available.
Perch Lake Mounds. 84p.12pl. Apr. 1905. Out of print.
Aboriginal Use of Wood in New York. t1gop. 35pl. June 1905.
Not available.
108 Aboriginal Place Names of New York. 336p. May 1907. 4o0c.
113 Civil, Religious and ae Councils and Ceremonies of Adop-
tion. rEsp,.7pl:. ‘Junes 1907, -25
a17. Parker, A.C. An: Erie aes Village and Burial Site. r1o2p. 38pl.
Deco 1907 1-: 30e:
125 Converse, H. M. & Parker, A.C. Iroquois Myths and Legends. 1g96p.
i crple Dec. 2906.5, 0c:
144 Parker, A. C. Iroquois Uses of Maize and Other Food Plants. t12o0p.
il. 31pl. Nov. 1910. Not available.
163 The Code of Handsome Lake. 144p. 23pl. Nov. 1912. Not available.
The Constitution of the Five Nations. In press.
Miscellaneous. 62 Merrill, F. J. H. Directory of Natural History Museums
in United States and Canada. 236p. Apr. 1903. 30¢.
66 Ellis, Mary. Index to Publications of the New York State Natural
History Survey and New York State Museum 1837-1902. 418p. . June
1903. 75¢, cloth.
Museum memoirs 1889-date. 4to.
t Beecher, C. E. & Clarke, J. M. Development of Some Silurian Brachi-
opoda. g6p. 8pl. Oct. 1889. $1.
2 Hall, James & Clarke, J. M. Paleozoic Reticulate Sponges. 35o0p. il. 7opl.
1898. $2, cloth.
3 Clarke, J. M. The Oriskany Fauna of Becraft Mountain, Columbia Cox
Nev a eeepecoply (Octs 1900... Soc:
4 Peck, C. H. N. Y. Edible Fungi, 1895-99. 106p. 25pl. Nov. 1900. WNot
available.
This includes revised descriptions and illustrations of fungi reported in the 49th, 51st and
52d reports of the State Botanist.
5 Clarke, J. M. & Ruedemann, Rudolf. Guelph Formation and Fauna of
New York State. 1096p. 2tpl. July 1903. $1.50, cloth.
6 Clarke, J. M. Naples Fauna in Western New York. 268p. 26pl. map.
1904. $2, cloth.
7 Ruedemann, Rudolf. Graptolites of New York. Pt 1 Graptolites of the
Lower Beds. 350p. 1r7pl. Feb. 1905. $1.50, cloth.
& Felt, E. P. Insects Affecting Park and Woodland Trees. v.1. 46op.
il. 48pl. Feb.1906. $2.50, cloth; v.2. 548p. il. 22pl. Feb. 1907. $2, cloth.
9 Clarke, J. M. Early Devonic of New York and Eastern North America.
Pie 4200p. il, zopl: 5amaps: Mar. roo8. $2.90, \clotit; Pte. 25op, 1236p.
4 maps. Sept. 1909. $2, cloth.
ro Eastman, C. R. The Devonic Fishes of the New York Formations.
2360p. F5pl. 1907. $1.25, cloth.
tr Ruedemann, Rudolf. Graptolites of New York. Pt 2 Graptolites of
the Higher Beds. 584p. il. 31pl. 2 tab. Apr. 1908. $2.50, cloth.
12 Eaton. Birds of New York. -v..7: Sorp.il. 4epl., “Apre rose.
$3, cloth; v. 2, 719p. il. 64 pl. July 1914. $4, cloth.
13 Whitlock, H.P. Calcitesof New York. 1gop. il.27pl. Oct. 1910. $1, cloth.
14 Clarke, J. M. & Ruedemann, Rudolf. The Eurypterida of New York. v. 1.
Text. 440p. il. v. 2 Plates. 188p. 88pl. Dec. 1912. $4, cloth.
Natural History of New York. 3ov. il. pl. maps. 4to. Albany 1842-94.
DIVISION 1 ZooLoGy. De Kay, James E. Zoology of New York; or, The
New York Fauna; comprising detailed descriptions of all the animals
hitherto observed within the State of New York with brief notices of
those occasionally found near its borders, and accompanied by appropri-
ate illustrations. 5v.il.pl.maps. sq. 4to. Albany 1842-44. Out of print.
Historical introduction to the series by Gov. W. H. Seward. 178p. J
87
89
THE UNIVERSITY OF THE STATE OF NEW YORK
v. 1 ptr Mammalia. 131 + 46p. 33pl. 1842.
300 copies with hand-colored plates.
Via pt2 Birds.! \\i2:>-)ss0pyerpupl ese,
Colored plates.
v. 3 pt3 Reptiles and Amphibia. 7+ 98p. pt4 Fishes. 15 + 415p. 1842.
pt 3-4 bound together.
v. 4 Plates to accompany v. 3. Reptiles and-Amphibia. 23pl. Fishes»
7opl. 1842.
300 copies with hand-colored plates.
v.5 pts Mollusca. 4+ 271p. 4gopl. pt 6 Crustacea. jop.13pl. 1843-44.
Hand-colored plates; pts—6 bound together.
DIVISION 2 BOTANY. ‘Torrey, John. Flora of the State of New York; com-
prising full descriptions of all the indigenous and naturalized plants hith-
erto discovered in the State, with remarks on their economical and medical
properties. av. il. pl. sq. 4to. Albany 1843. Out of print.
v. 1 Flora of the State of New York. 12 + 484p. 72pl. 1843.
300 copies with hand-colored plates. .
v. 2 Flora of the State of New York. 572p. 89pl. 1843.
300 Copies with hand-colored plates.
DIVISION 3 MINERALOGY. Beck, Lewis C. Mineralogy of New York; com-
prising detailed descriptions of the minerals hitherto found in the State
of New York, and notices of their uses in the arts and agriculture. il. pl.
sq. 4to. Albany 1842. Out of print.
v. 1 ptr Economical Mineralogy. ptz Descriptive Mineralogy. 24 + 536p.
1842. :
8 plates additional to those printed as part of the text.
DIVISION 4 GEOLOGY. Mather, W. W.; Emmcns, Ebenezer; Vanuxem, Lard-
ner & Hall, James. Geology of New York. 4v. il. pl. sq. 4to. Albany
1842-43. Out of print.
1 ptr Mather, W. W. First Geological District. 37 + 653p.46pl. 1843.
2 pt2 Emmons, Ebenezer. Second Geological District. 10 + 437p.
r7pl. 1842.
. 3 pt3 Vanuxem, Lardner. Third Geological District. 306p. 1842.
4 pt4 Hall, James: Fourth Geological District. 22 + 683p. 1gpl.
map. 1843.
DIVISION 5 AGRICULTURE. Emmons, Ebenezer. Agriculture of New York;
comprising an account of the classification, composition and distribution
of the soils and rocks and the natural waters of the different geological
formations, together with a condensed view of the meteorology and agri-
cultural productions of the State. 5v. il. pl. sq. 4to. Albany 1846-54.
Out of print.
v. x Soils of the State, Their Composition and Distribution. 11 + 371p. 21pl.
18406.
v. 2 Analysis of Soils, Plants, Cereals, etc. 8 + 3434+ 45p. 42pl. 1849.
Viith hand-colored plates.
v. 3 Fruits; ete: 8 4 3240p.) 1852.
v. 4 Plates to accompany v. 3. g5pl. 1851.
Hand-colored.
v. 5 Insects Injurious to Agriculture. 8 + 272p. 5opl. 1854.
With hand-colored plates.
DIVISION 6 PALEONTOLOGY. Hall, James. Paleontology of New York. 8v.
il. pl. sq. 4to. Albany 1847-94. Bound 1n cloth.
v. 1 Organic Remains of the Lower Division of the New York System.
23 + 338p. oopl. 1847. Out of print.
v. 2 Organic Remains of Lower Middle Division of the New York System.
8 + 362p. rogpl. 1852. Out of print.
v. 3 Organic Remains of the Lower Helderberg Group and the Oriskany
Sandstone. pt1, text. 12 + 532p. 1859. [$3.50]
pt 2. r42pl.) 78657, [S2u501
nos
<<
MUSEUM PUBLICATIONS
v. 4 Fossil Brachiopoda of the Upper Helderberg, Hamilton,. Portage and
Chemung Groups. 11 + 1+ 428p.69pl. 1867. $2.50.
v. 5 pt x Lamellibranchiata 1. Monomyaria of the Upper Helderberg,
Hamilton and Chemung Groups. 18 + 268p. 45pl. 1884. $2.50.
Lamellibranchiata 2. Dimyaria of the Upper Helderberg, Ham-
ilton, Portage and Chemung Groups. 62 + 293p. 51pl. 1885. $2.50.
pt 2 Gasteropoda, Pteropoda and Cephalopoda of the Upper Helder-
berg, Hamilton, Portage and Chemung Groups. 2v. 1879. v. 1, text.
ey 4 402p.; V.2. r2opl, 2.50: for 2 v.
& Simpson, George B. v. 6 Corals and Bryozoa of the Lower and Up-
per Helderberg and Hamilton Groups. 24 + 298p. 67pl. 1887. $2.50.
—— & Clarke, John M. v. 7 Trilobites and Other Crustacea of the Oris-
kany, Upper Helderberg, Hamilton, Portage, Chemung and Catskill
Groups. 64 + 236p.46pl. 1888. Cont. supplement tov.5,pt2. Ptero-
poda, Cephalopoda and Annelida. 42p.18pl. 1888. $2.50.
& Clarke, John M. v.8ptxz Introduction to the Study of the Genera
of the Paleozoic Brachiopoda. 16 + 367p. 44pl. 1892. $2.50.
& Clarke, John M. v.8 pt 2 Paleozoic Brachiopoda. 16 + 394p. 64pl.
1894. $2.50.
Catalogue of the Cabinet of Natural History of the State of New York and
of the Historical and Antiquarian Collection annexed thereto. 242p. 8vo.
1853. Out of print.
Handbooks 1893-date.
New York State Museum. 52p. il. 1902. Free.
Outlines, history and work of the museum with list of staff 1902.
Paleontology. 1312p. 1899. Out of print.
Brief outline of State Museum work in paleontology under heads: Definition; Relation to
biology; Relation to stratigraphy; History of paleontology in New York.
Guide to Excursions in the Fossiliferous Rocks of New York. 124p. 1899.
Free.
Itineraries of 32 trips covering nearly the entire series of Paleozoic rocks, prepared specially
for the use of teachers and students desiring to acquaint themselves more intimately with the
classic rocks of this State.
Entomology. 16p. 1899. Out of print.
Economic Geology. 44p. 1904. Free.
Insecticides and Fungicides. 20p. 1909. Free.”
Classification of New York Series of Geologic Formations. 32p. 1903. Out
of print. Revised edition. 96p. 1912. Free.
Geologic maps. Merrill, F. J. H. Economic and Geologic Map of the
State of New York; issued as part of Museum Bulletin 15 and 48th Museum
Report, v. 1. 59x67 cm. 1894. Scale 14 miles to 1zinch. 165¢c.
Map of the State of New York Showing the Location of Quarries of
Stone Used for Building and Road Metal.: 1897. Out of print.
Map of the State of New York Showing the Distribution of the Rocks
Most Useful for Road Metal. 1897. Out of print.
Geologic Map of New York. t1go1. Scale 5 miles to r inch. In atlas
form $2. Lower Hudson sheet 60c.
The lower Hudson sheet, geologically colored, comprises Rockland, Orange, Dutchess,
Putnam, Westchester, New York, Richmond, Kings, Queens and Nassau counties, and parts
of Sullivan, Ulster and Suffolk counties; also northeastern New Jersey and part of western
Connecticut.
Map of New York Showing the Surface Configuration and Water Sheds.
1901. Scale 12 miles to 1 inch. 15¢c.
Map of the State of New York Showing the Location of Its Economic
Deposits. 1904. Scale 12 miles to 1 inch. 1§5¢c.
Geologic maps on the United States Geological Survey topographic base.
Scale 1 in. = 1 m. Those marked with an asterisk have also been pub-
lished separately.
*Albany county. 1898. Out of print.
Area around Lake Placid. 18098.
Vicinity of Frankfort Hill [parts of Herkimer and Oneida counties]. 1899.
THE UNIVERSITY OF THE STATE OF NEW YORK
Rockland county. 1899.
Amsterdam quadrangle. 1goo.
*Parts of Albany and Rensselaer counties. t1gor. Out of print.
*Niagara river... 1o90r,' 252.
Part of Clinton county. tgor.
Oyster Bay and Hempstead quadrangles on Long Island. 1oor.
Portions of Clinton and Essex counties. 1go2.
Part of town of Northumberland, Saratoga co. 1903.
Union Springs, Cayuga county and vicinity. 1903.
*Olean quadrangle. 1903. Free.
*Becraft Mt with 2 sheets of sections. (Scale 1 in.==im.) 1903. 20c
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Paradox Lake quadrangle. 1905.
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*Attica-Depew quadrangles. I914. 20c.
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