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70

University of the State of New York

BULLETIN

OF THE

New York State Museum

VOL. 5 No. 21

SEPTEMBER 1898

GEOLOGY

OF. THE

LAKE PLACID REGION

BY

JAMES FURMAN KEMP, E. M.

Prepared with the permission of Prof. James Hall, State Geologist, and Charles D. Wolcott,

M4z2m-Jlg8=1500

Director U. S. Geological survey

ALBANY
UNIVERSITY OF THE STATE OF NEW YORK
1898 Price 5 cents

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CONTENTS

PAGE
Mimo UC hOMpeIas secs eerie rece. ce sss wce as seca neice \elnana cess) a clsne ehcleee 51
EOE MICHOUbIIMNE ta taemee se sie scence s Soc ccee Seis soe eae cise ae co scyoaee 51
ISOGES oo onacoe ooadoo SS sdce DOSHGS Hpac USS seq ceGooU Boonen gona noacmaRDGoce Haas 53
GavsrnlimoswmestOnests. =. cess sce e esas soles vec nitt ke leca dls seaee does 53
Quartzite ........ SO RO CISHO CIAO CDS RESO eRroC hho GUA ASE OEE CAME emcod Srac 54
(ANN UO Wem site asic cre elas Sataicisve leas cise Selciseie amenieleci ae sda coe secs ee 54
(CMGNES, - nosuso sooo sodeededd sso sdooas sdabeS cons coon sedoUa eEseao osoccess 55
AVTOMMACRUGE) sSanes anode coobds so SHOOISEOD 000 565 BAe nO S RIPE REBeIsOOoEOwace 57
TDD (USGS). oSh2 se Sone cost pee ded Codees Boos Sat cOnReGe Be emEeah Shes oone 58
NIGTAIGS 9 SoS8 Gash COdn Bee RO RIGS CE SIDOUOOC. SUC a> See Anan eee ss Gtas 59
Wraiter-sortedisands and gravels -o2.)2- 52 -co- cos ocieclenes 20s once ceeeee 59
CEOIOGIO DE@y< 55. co0c 0506 pbanoo ep shoo cosont Gabo EonsopEeeeASpopeon ooHede 60
Relief map—based on the Lake Placid and Mt Marcy sheets of the U.S.
SENOGICA RINT OMe sho Gon quae cOaeo bese Us co Se COE C Osea aU Ce beea SeSeeo opp. p. 62
NEUSE Say tek Ge cee 6 SO ee ee ee ee ee 63
Geologie map of the area around Lake Placid................--. seecoverp. 2
[Nirxel Gceeenge rete eee ee ree ae eicicta sis nie sinbaicicare's, alsteiciciele s\oc'a'a! ecle civinjicain sis seitiere 65

iy De

GEOLOGY OF THE LAKE PLACID REGION

INTRODUCTION

The following outline of the geology of the region about Lake
Placid has been prepared from notes which were taken while the
writer was in the field, first under the direction of Prof. James
Hall, state geologist and later under that of Dr Charles D. Wal-
cott, director of the United States geological survey. Acknowl-
edgments are due both these gentlemen for permission to use the
observations.

It has been the writer’s aim to give an observer, and specially
a teacher who might be sojourning in the region, a grasp of its
larger geologicfeatures,and tosuggest the topicsinregard to which
our present knowledge needs amplification. The writer’s attention
has been thus far chiefly centered on the hard crystalline rocks as
distinguished from the incoherent sands, gravels and moraines
that rest on them. Much remains to be done in the study of
these last named, for they give the clue to the recent geologic
history of the valley and by a careful study of them and by dis-
tinguishing moraines, deltas, abandoned lake bottoms and their
respective altitudes some interesting problems in geographic
geology may be solved.

GEOGRAPHIC OUTLINE

If an observer stands on an elevated point near Lake Placid,
with the relief map which will be found opposite p. 62 in hand he
will note that the region about him lies to the northwest of the
great central group of peaks, which constitutes the backbone of
the Adirondacks. The Gothics, Marcy, McIntyre and their neigh-
bors form the southeastern sky line and a broad, open valley lies
between their foothills and the lake itself. Whiteface, one of
the highest peaks bounds the lake on the north and with its
spurs incloses the valley in this direction. Beyond White-
face, the mountains decrease rapidly in size, and although
for many miles the country is wild and rugged, the altitudes
gradually decline to the plain that forms the south bank of the

52 NEW YORK STATE MUSEUM

St Lawrence river. The eastern side of the Lake Placid valley is
chiefly formed by the fine massif of Sentinel mountain, whose
northwestern spur is cleft from Mt Whiteface by the Wilmington
Notch, and whose southern is similarly separated from Pitchoff
mountain by the narrow pass through which runs the old but
now abandoned road to the Keene valley. Pitchoff is in turn
split off from Cascade and Porter mountains by the Cascadeville
Notch, likewise a precipitous pass. It may be farther remarked
that if one goes out to the south one must take the trail through
Avalanch pass, another narrow cleft in the mountains, or else the
still more famous Indian pass, which lies on the west side of Mt
McIntyre, and which is in many respects the most impressive of
all the Adirondack passes.

To the west the country is more open, and in driving to
Saranac, a broader valley with much lower hills surrounding
it is met. The present lack of topographic maps of this section
has prevented its accurate study as yet, although its character
can readily be seen by a drive or a walk.

The drainage of the Lake Placid valley passes out through the
west branch of the Ausable river and enters Lake Champlain
through the famous Ausable chasm, just north of Port Kent. The
valley lies therefore in the St Lawrence drainage basin, but is near
its southern limit. The headwaters of the Hudson are in
Avalanch pass a few miles to the south.

In its smaller features the valley south of Lake Placid is to a
great degree a plain of sand and gravel, now quite deeply dis-
sected by the various streams which cut across it. Flat-topped
hillocks, the stumps of the former general level remain and
enable one to fill out its former conditions. Occasional moraines
of sand and boulders, such as the one on which the Lake Placid
hotels are built, diversify the surface, but the general aspect is
that of a plain, whose relief is due to erosion.

The altitude of the lake above tide is 1864 feet. The West
Branch at the High Fall is 1800 feet and at Wilmington village
1000, so that the rapid fall of the river explains the great amount
of erosion that has been accomplished. The altitudes of the

GEOLOGY OF THI LAKE PLACID REGION 53

several peaks in the immediate vicinity are as follows: White-
face, 4872; Sentinel, 3858; Pitchoff, 3450; Cascade, 4092; Por-
ter, 4070. Mt McIntyre, at 5112, can be reached and ascended in
a day, and is second only to Mt Marcy at 5344. Of all the Adi-
rondack peaks, these two alone, McIntyre and Marcy, exceed
5000 feet but several others approximate it closely.

Of the minor elevations near the lake, Eagle Eyrie is 2656,
Pulpit mountain 2658, the two being practically the same, and
Cobble hill is 2330.

ROCKS

The rocks proper, which include the ‘ hard’ formations as con-
trasted with the incoherent sands and gravel, may be classified
into 1) crystalline limestone, 2) quartzite, 8) granite, 4) gneiss,
5) anorthosites or the rocks consisting chiefly of labradorite feld-
spar, 6) trap dikes. If we add the incoherent sands and gravels,
there are,.7) moraines of unsorted sands and boulders, large and
small being commingled, and 8) water-sorted sands and gravels,
forming abandoned lake bottoms and deltas now more or less
modified by erosion both by wind and water.

Crystalline limestone. This rock is not in large amount but
it is extremely significant in its geologic relations. Reference
to the geologic map (cover p. 2) will indicate its presence in only
one place so far as known in the town of North Elba and that is
near the trail that leaves the Wilmington road at the house of
Mr Watson. A small area outcrops in the bottom of a brook. In
the valley of the east branch of the Ausable river, one outcrop
occurs in the town of Jay. There are at least six or seven in
Keene. The limestone is always a coarsely crystalline variety,
and is formed of rather large individuals of calcite, through
which smaller crystals of pyroxene, of the variety coccolite, are
richly distributed in practically all cases. Graphite is often
present and dark bunches of varying size consisting of black
hornblende, quartz, pyrrhotite, feldspar and some rarer minerals
are frequent. Traces of bedding have been destroyed and al-
though the limestone shows as a rule a banded character, this
is the result of pressure exerted during its metamorphism. The

54 NEW YORK STATE MUSEUM

invariable presence of the pyroxene and other silicates leads us
to infer that the original limestone was an impure siliceous
variety, and when metamorphism affected it, the silica, lime,
magnesia and iron present, became combined in the included min-
erais. The limestones furnish the only localities attractive to
the collector of minerals and some advice regarding them is
given later under the head of mineralogy (p. 63). In fact loose
bunches of pyroxene crystals, garnets and other characteristic
aggregates and masses of black hornblende often remind us when
doing field work that limestones must be near before the actual
outcrop is discovered.

Quartzite. In two or more localities small outcrops have been
met of a rock that seems to be excessively altered sandstone. One
is on the old road from North Elba to Keene, and is in Keene town-
ship; the other is at the Red Rocks on the east side of the Keene
valley. Additional ones of small size are met in a minor degree as-
sociated with the limestones of the Keene-Jay valley. The rock
appears to the unaided eye to be an aggregate of little else than
quartz grains through which flakes of graphite may occasionally
be detected. When cut in thin section the rock from the
old Keene road shows much emerald green pyroxene, and a
little scapolite. AJl the minerals are strained and fractured and
have clearly been subjected to great pressure. The outcrops
in the two localities specially cited are in or near steep precipi-
tous cliffs, that have been produced by faults.

The quartzites were doubtless originally sandstones that had
sometimes carbonaceous matter, and sometimes lime, magnesia,
iron and alumnia, sufficient in amount to yield the acces-
sory minerals. Along the old Keene road the quartzite passes
almost imperceptibly into a gneiss, that may itself be an altered
sediment.

Granite. In four localities a rock has been met that corres-
ponds to granite. One is on the steep sides of a spur of Mt White-
face along the trail from the north end of Lake Placid to Franklin
Falls. Another is at the High Falls in Wilmington Notch in the

GEOLOGY OF THE LAKE PLACID REGION 55

bed of the stream. A third is in a hill a mile east of Scotts Cob-
ble, and the fourth is in the bed of the East Branch at the cas-
cade between Keene Center and the iron bridge a mile and a half
south. In each case the rock is chiefly quartz and feldspar, in a
coarsely crystalline aggregate. In thin section the quartz is
found to be much strained from geologic movements, and the
feldspar is the variety microperthite, being an orthoclase thickly
set with little spindles of albite.

The three rocks above referred to, and the trap dikes to be
later described are minor rock formations, nearly all the country
being made up of the two that follow next.

Gneiss. Under this comprehensive name is included a consid-
erable variety of rocks, all of which have however the distin-
guishing feature of ‘ gneiss’ in strong development. That is; the
light and dark minerals are arranged in rudely parallel bands so
as to give a foliated or laminated aspect to the rock. The

banding varies from coarse to fine, and is produced by innumer-
able flattened lenses of minerals, strung out with their long
diameters parallel. The bands curve and eddy at times and
strongly simulate the phenomena produced by the flow of a ropy
or viscous fluid. :

The commonest gneiss is a dark, and more or less rusty rock,
with abundance of black minerals, set in a brown or green
mass of feldspar. When a fresh exposure is produced either by
pounding to the core of a large fragment or in blasting boulders
and ledges for the improvement of highways, it is seen that the
rock is a pronounced green. Red garnets are frequently quite
prominent in it. In thin sections this variety is found to be
chiefly composed of microperthitic feldspar and emerald green
pyroxene. With these in places here and there are varying
amounts of hornblende, hypersthene, quartz, garnet, magnetite
apatite and zircon. When the quartz is abundant, varieties high
in silica result; when it and the feldspar are in less amount, dark
pyroxenic and hornblendic varieties occur in consequence.

In some gneisses large blue labradorites are quite prominent,
but always in rudely lenticular form, giving the general impres-

56 NEW YORK sTATE MUSEUM

sion of an eye, around which the dark minerals are ranged like
eyelashes and eyebrows. For this reason it is customary to des-
cribe the labradorites as ‘ Augen’ using the German word for
eyes. They indicate relationships with the anorthosites, the next
group of rocks.

The obscure geologic questions that arise in connection with
the gneisses are those which deal with their original condi- —
tion and the changes through which they have passed to reach
their present condition. The gneisses are essentially ‘ meta-
morphic’ rocks, and the term means that by recrystallization
or by compression, crushing and consequent internal movye-
ments, or by both combined, they have been produced from
sediments or from igneous rocks. It was formerly believed
that the foliation represented the bedding of sediments, but it
seems now more reasonable to regard it as the result of pressure
and of a movement analogous to a viscous flow, that has strung
out the minerals in lines. It is quite probable that some of the
gneisses and specially those associated with the limestones and .
quartzites are altered sediments, and it is also probable that
those with the labradorite augen are squeezed igneous rocks, but
our investigations do not yet admit of their separation in map-
ping. '

The gneisses are colored brown on the map, by reference to
which it will be seen that they bound Lake Placid on the east
and appear to some extent in the islands on the east side. Excel-
lent exposures with pronounced foliation will be found in the
cliffs of Pulpit mountain, on Eagle Kyrie and in Sunrise Notch.
Along the West Branch they are the country rock. Pitchoff
mountain and the southwest portions of Sentinel are composed
of them and the ledges on the East Branch in Jay and northern
Keene are the same. The boundaries between them and the anor-
thosites are not sharp and passage forms are met so that the
areal distribution on the contacts is approximate. Repeated ex-
perience has, however, indicated both to the writer in Essex
county, and to H. P. Cushing in Franklin county that dark
gneisses with labradorite augen, often surround areas of anor-

GEOLOGY OF THE LAKE PLACID REGION 57

thosite and that the transition from one to the other is a gradual
one.

Anorthosites. The anorthosites may be considered to be the
characteristic rocksof the Adirondacks. In their typical cases they
consist of little else than blue labradorite and are then a most
beautiful rock. A little pyroxene, mostly augite, appears as a rule,
and hypersthene is frequent. The presence of the latter led Prof.
Emmons in the early work of the New York state survey to call
them hypersthene rock, or hypersthene, but this mineral is a
subordinate one. Labradorite is the great component and the
rocks might be fittingly described as ‘ labradorite rocks’, follow-
ing a custom prevalent in Norway, but in English the term is not
a good rock name. They are sometimes described as norite
meaning a rock composed of labradorite and hypersthene, but
experience has indicated the scarcity of hypersthene, and here
the word anorthosite is employed, which means a rock chiefly
composed of plagioclase feldspar. The rocks resemble a coarse
granite, the individual crystals being sometimes very large.

The typical anorthosites grade into varieties with more and
more dark silicates and some of the areas colored red on the map
have large and prominent amounts of them. These darker
pyroxenic and hornblendic rocks are not anorthosites, strictiy
speaking but are gabbros and diorites; nevertheless the anor-
thosite is the prominent and characteristic variety and is here
used with that understanding. The summit of Mt Whiteface and
the southern portion of the mountain consists of a variety that
contains large amounts of hornblende and pyroxene, together with
milky white feldspar. It is so peculiar that we have been accus-
tomed in the field to refer to it as the Whiteface type of rock. It
is characteristic of this mountain ridge. Despite the peculiarities
of the rock, it belongs beyond question in the anorthosite series,
and is closely involved with typical anorthosites. The latter are
found all around the base of the mountain toward Wilmington
and on the trail from Wilmington village, to the summit, that
passes over Marble mountain, typical anorthosites appear till
the peak is nearly reached.

58 NEW YORK sTATE MUSEUM ESE

The anorthosites have not escaped the general results of
squeezing and crushing that are so strongly shown by the
gneisses. On the contrary the feldspar crystals in the area of
the map are seldom if ever provided with sharp edges. A blue
crystalline nucleus is surrounded by a crushed white pulp of
comminuted feldspar, phenomena that will forcibly appeal to
an observer as having been produced by pressure on a grand
scale. They are also drawn out into gneissoid foliation in many
instances, but this structure is not specially marked because of
the lack of dark minerals, which accentuate it by contrast with
the feldspar. Often a narrow rim of pink garnets will be noticed
surrounding such dark silicates as appear in the anorthosite.

The anorthosites in typical development will be found on the
west side of Lake Placid, and specially on the hilltop back of the
Whiteface Inn. As the Whiteface type they constitute the peak
of the same name. They bound the Wilmington valley so far as
here mapped, and make up all the central part of the Sentinel
range. To the south they become the prevailing rock and beyond
the area of the map they form all the high peaks around Mt Marcy.

Trap dikes. The trap dikes constitute minor but striking mem-
bers in the geology of the region. They are not numerous so far
as known within the area of the map. They have been met almost
always throughout the mountains, where some great fault line
has formed a line of weakness, up through which they have
found an outlet from the reservoirs of molten rock in the in-
terior. They are all black basalt and in thin section are shown
by the microscope to contain plagioclase feldspar and augite, as
the most abundant minerals. Magnetite, apatite and sometimes
brown hornblende are also present, and more or less glass.

A dike occurs about a mile north of Eagle Eyrie. A ramifying
and very instructive network of them is well exposed at the High
Fall in Wilmington Notch. Others were noted in the limestone
area a mile or so south of the Notch proper. They occur north-
west of Clifford Falls on the east slope of Sentinel. In the Cas-
cade Notch, immediately opposite the hotel and beneath the
‘cascade’ there is another network of them, and still another in

GEOLOGY OF THE LAKE PLACID REGION 59

the gorge of the East Branch a mile south of Keene Center. No
doubt additional ones will be discovered by observation of the
brook bottoms and the writer would be glad to be informed of
any that may be met.

Moraines. The moraines of unsorted sand and boulders are
the most striking evidence of the glacial period. They meet the
eye of the visitor immediately on reaching Lake Placid, because
the town is built upon a ridge formed of them. Huge boulders
preject from the sides of cuttings wherever the highways have
been graded. This commingling of large rocks and fine sands
will appeal even to the unscientific observer as only to be ex-
plained by the work of ice. This particular moraine is an im-
portant one because Lake Placid is the result of it. Like a great
dam the glacial drift confines the water to the valley between
the hills, while Mirror lake is in a depression in the dam itself.

Other moraines are not lacking in the region but as our obser-
vations are as yet too incomplete to accurately map them no dis-
tinction is made on the map. Some minor points of interest may
however be mentioned. In the pass toward French’s at the
north end of Lake Placid, and beyond Eagle Kyrie, there is a
huge boulder that is 25x 20x15 feet, as determined by pacing.
It stands by itself in the forest. Others of notable size are
abundant on the hillsides south of Keene Center. The boulder
at John Brown’s grave is one of the sights familiar to the Lake
Placid summer visitor.

The boulders in the moraines are chiefly the hard crystalline
rocks already described. Occasionally one finds a fragment of
Potsdam sandstone, that must have journeyed in from many
miles to the north.

Water-sorted sands and gravels. These consist of pebbles
and sand in a more or less clearly stratified condition. They
tend specially to form level plains and fan shaped terraces. The
plains appear to be abandoned lake bottoms, while the terraces
are the deltas which entering streams built up in the former
lakes. The deltas occur opposite the tributary valleys and

60 NEW YORK STATE MUSEUM

specially in the Keene valley, two or three distinct sets can be
recognized. Similar phenomena on a small scale can be recog-
nized in the present lakes.

The open valley south of Lake Placid gives much evidence of
having once been a lake whose waters were held in, perhaps by an
ice wall to the north. As earlier stated the stumps of the sandy
plain, and the deltas need to be correlated as regards altitudes
before we can be sure of the conditions surrounding the former
lake. The valley in which the town of Wilmington lies is a strik-
ing case of a lake basin, and not less significant are the lake bot-
toms and deltas in the Keene valley and in the Elizabethtown
valley. The latter is almost diagrammatic.

Geologic age. The hard crystalline rocks are of pre-Cam-
brian age, with the possible exception of the trap dikes. If the
word archean is used in the original sense as proposed by the late
Prof. Dana, for the formations that precede the fossiliferous
strata, then the Lake Placid crystallines are archean. But if,
as has been more recently proposed by the United States geologi-
cal survey, the name archean is restricted to those ancient rocks
that antedate all sediments, then the local formations must be
called Algonkian, a name that applies to pre-Cambrian rocks that
are sedimentary, or, if igneous, that are later than known sedi-
ments. ee

The name Laurentian has been widely employed for the ancient
crystalline rocks in the text-books on geology, and as it was origi-
nally used in Canada for rocks geographically and geologically
related to those under consideration here, it may be referred to.
The Canadian geologists introduced the name Laurentian for the
oldest crystalline rocks of the globe, and set off from them under
the name Huronian, the metamorphosed sediments and igneous
rocks that rest upon the Laurentian around Lakes Superior and
Huron. With the exception of the trap dikes, the Lake Placid
rocks are all Laurentian, but no Huronian rocks are known in the
region.

Fairly extended observation throughout the Adirondacks has
led to the conclusion that the limestones, quartzites and probably

GEOLOGY OF THE LAKE PLAOID REGION 61

some of the gneisses are the oldest rocks present. They repre-
sent the remnants of a once extended series that formed all the
country. They have been invaded and broken up into small de-
tached areas by the igneous anorthosites. The intrusions took
place at quite profound depths in the earth, because the anortho-
sites have all the characteristics of rocks that have cooled and
crystallized under pressure and slowly. The limestones were
much affected by the neighboring masses of igneous rock and may
owe to their influence the great numbers of included pyroxenes
and other silicates.

Many facts otherwise inexplicable are accounted for by this
conception, as for instance the presence opposite Cascadeville of a
small mass of limestone, a sedimentary rock, in a great mountain
of anorthosite, an igneous one. The limestone on the north-
western extremity of Pitchoff is a still more striking case, while
fragments of quartzite have been found in the anorthosites of the
high peaks, as for instance on the summit of the Gothics. The
exact relations of the granites to the anorthosites in time, are
uncertain, but the granites are probably later.

After the intrusion of the anorthosites great metamorphism
ensued, that crushed the component minerals and produced much
gneissoid foliation. The rocks were apparently under such com-
pression and strain, that they flowed like a viscous fluid, and the
minerals became strung out in linear arrangement. It all
occurred however before the deposition of the Potsdam sand-
stone, because we find the latter to the north and east resting
unchanged on the older metamorphic rocks.

The trap dikes were certainly intruded after the metamor-
phism, for they show no evidence of having been squeezed or
Sheared. In the region to the north, H. P. Cushing has found
dikes that cut the old crystallines, but stop at the Pots-
dam, and do not penetrate it. He therefore has concluded that
they were intruded before the Potsdam was deposited. The
writer has found others in the Lake Champlain region that
pierce strata even as late as the Utica slate. Clearly therefore
two series are present in the mountains, but to which of the two

62 NEW YORK STATE MUSEUM

the dikes around Lake Placid belong, we can not say from the
local evidence.

‘As to what took place in this region in the long interval of time
represented by the paleozoic and mesozoic eras and the tertiary
period, we can but imagine and most imperfectly. Whether the
mountains were leveled off, submerged and buried under strata
that have since been removed, or whether they were a land
area, that suffered great denudation and furnished material for
later sediments, we have slight means of knowing. For the later
paleozoic and for the mesozoic and tertiary the latter supposition
is the more reasonable. Careful study of the physiography may
throw some light on the tertiary or even on the later mesozoic
times, if remnants of old drainage systems can be made out. Pre-
sumably their outlines were not so very different from the pres-
ent ones. ;

At some time in this interval the great faults were developed
that have served to block out the individual mountains and val-
leys and that are the primary causes of the relief and of the
present drainage.. The crushing of the rocks from the faulting
gave the rivers their easiest lines of erosion. This inference is
corroborated by the cracked and jointed condition of the rocks
in the channels, where exposed, and by the steep, precipitous
cliffs in the passes, which are due to the scaling off of platy
masses along the old lines of fracture. These movements may
have occurred in quite recent geologic time, but in no case have
we found faulted glacial deposits. ;

With the opening of the quaternary period came the invasion
of the continental glacier and the production of the moraines,
boulders and beautiful. glacial amphitheaters or cirques on the
slopes of Whiteface and Sentinel. The boulders of Potsdam
sandstone indicate a movement from the northeast, and the few
glacial striae that have been met corroborate the inference. They
are not common in the area of the map and should be looked for
with care and their directions should be taken with a compass.

The configuration of the mountain slopes is strikingly charac-
teristic of ice action, and if the reader will observe on the relief

GEOLOGY OF THE LAKE PLACID REGION 63

map, opposite p. 62, the eastern front of Whiteface for example,
he will be impressed with the amphitheaters, setting back
against precipitous walls, that are everywhere present. The
same is true of Sentinel mountain about the headwaters of Clif-
ford brook. Ice appears to have stood in these recesses and to
have worked the sides back to the comparatively steep walls
which confront us to-day. The open space or ‘ bergschrund ’, that
usually intervenes as a huge crack between the ice of a glacier
and its inclosing wall, is a place of specially active disintegration
of rock. The thaw by day is succeeded by freezing during the
night and the walls scale off to a fairly vertical condition with ex-
ceptional rapidity. ‘An amphitheater with steep walls results,
' which is a favorite form for the Adirondacks, being well shown on
Giant, on the Gothics and not a few other peaks.

The melting of the ice sheet and its retreat, the temporary
blocking of lines of drainage and perhaps general submergence of
the region led to the production of lake basins, with their attend-
ant deltas and sand plains, now a most suggestive feature of the
landscape, but observations, as already stated, have not yet been
made in sufficient detail to work out their number, succession
and relative altitudes.

MINERALOGY

The larger formations present little that is attractive to the
collector of minerals. The labradorite crystals of the anortho-
sites occasionally reach such dimensions and perfection of de-
velopment as to exhibit the characteristic twinning striations
on cleavage faces. Rarely they show the characteristic play of
colors of the labradorite from eastern Canada.

The included masses of limestone are much more prolific. At
Caseadeville beautiful light green coccolite is distributed
through white calcite. Small dark brown or black garnets are
associated, but neither the garnet nor the pyroxene possesses
good crystal boundaries, as the individuals have the rounded or
corroded aspect, so often seen on minerals contained in lime-
stone.

64 NEW YORK STATE MUSEUM

In earlier notices of this locality zircon and vesuvianite are
mentioned but the writer has been unable to find them. Mag-
netite with included pyrites is available near the Cascade.

At the Weston mine in Keene, magnetite, yellow and brown
garnets and pyroxene are quite abundant but the forms are rude
in outline. In limestone areas outside the limits of the map,
good crystals of pyroxene, titanite, hornblende and quartz can
sometimes be freed by acid from the inclosing calcite. They are
found in the bunches of silicates that are included in the lime-
stone even up to large size. Calcite and pyrite have also been
seen. They may all be found in the future in the outlying areas
of limestone shown on the map, and to these a collector may
most profitably direct his search.

INDEX

The superior figure points to the exact place on the page in ninths; e. g. 604 means four

ninths of the way down page 60.

_ Age of rocks, geologic, 604-637.

Albite, 552.

Algonkian formations, 60°.

Altitudes, 529-532,

Amphitheaters, glacial, 628.

Anorthosites, 534, 615, 637; age, 612;
characteristics and _ distribution,
571-58; relations to gneiss, 568.

Apatite, 558.

Archean, term, 604.

‘ Augen’ in labradorites, 559.

Augite, 572, 588.

‘Ausable chasm, 527.

Ausable river, east branch, crystalline
limestone, 537; gneisses, 567; granite,
551; trap dike, 591.

Ausable river, west branch, 526; de-
scent, 529; gneisses, 567.

Avalanch pass, 523, 527.

Basalt, 587.

Boulders, 592; near Lake Placid, 597;
of Potsdam sandstone, 628.

Brown, John, boulder at his grave, 597.

Calcite, 538, 639, 643.

Cascade mountain, 523; altitude, 531;
minerals, 641.

Caseade Notch, 523; trap dike, 589.

Cascadeville, limestone, 614, 639.

Clifford brook, glacial amphitheaters,
632.

Clifford falls, trap dike, 58%.

Cliffs, gneiss, 567; quartzite, 547.

Cobble Hill, altitude, 53%.

Coccolite, 538, 639.

Crystalline limestone, 534; distribu-

characteristics, 53°-543,
See also Limestones.

Cushing, H. P., conclusions, 569, 618.

tion and

Dana, J. D., use of word archean, 604,

Deltas, 53°, 599, 63°.

Dikes, distribution and characteristics,
582-591,

Diorites, 57°.

Drainage systems, old, 624; present,
62°.

Eagle Eyrie, altitude, 532; gneisses,
567; trap dike, 588.

East Branch, see Ausable river, east
branch.

Elizabethtown valley, lake bottoms,
603.

Emmons, Prof., opinion, 57°.

Fault, 547, 587, 625.

Feldspar, 539, 551, 557, 558, 581; plagio-
clase, 579-588.

Foliation, 55°; cause, 564, 617.

Franklin falls, granite, 549.

French’s, boulder, 59°.

Gabbros, 576.

Garnets, 542, 557, 583, 639, 642.

Geographic outline, 516, 532.

Geologie age of rocks, 604-637.

Giant mountain, glacial amphitheaters,
634.

Glacial amphitheaters, 631.

Glacial period, evidences of, 592, 628.

Glass, 588.

66 NEW YORK

Gneisses, 534, 548, 569; age, 611; char-
acteristics, 554-56°; distribution, 566
571; how produced, 562.

Gothies, 517; anorthosites, 61°; glacial
amphitheaters, 634; quartzite, 6L°.
Granite, 534; distribution and charac-

teristies, 549-553; age, 616.
Graphite, 538.
Gravel plains, 528.
Gravels, incoherent, 534.
Gravels and sands, water-sorted, 599-
603.

Hali, James, acknowledgments to, 512.

High Falls, altitude, 529; granite, 549;
trap dike, 589.

Hornblende, 539, 543, 558, 588, 642.

Hudson river, headwaters, 527.

Huronian rocks, 608.

Hypersthene, 558, 572.

Ice, action of, 632. See also Moraines.

Indian pass, 523,

Jay, gneisses, 567.

Keene, boulder, 597; crystalline lime-
stone, 537; gneisses, 568; granite,
551; quartzite, 544; Weston mine,
642,

Keene valley, abandoned road, 522;
deltas, 601; lake bottoms, 603.

Labradorite, 571, 637; ‘augen,’ 559.

Lake bottoms, abandoned, 535, 599,
603, 63°.

Lake Placid, age of trap dikes, 621; alti-
tude, 529; anorthosites. 584; boulder,
595; deltas, 602; drainage, 52°; evi-
dences of glacial period, 59%; geo-
logic age of rocks, 609;
567; topography, 51°.

Laurentian rocks, 607.

Limestones, 638; age, 60%.
Crystalline limestone.

gneisses,

See also

McIntyre, Mt, 517, 524; altitude, 531.
Magnetite, 558, 588, 641, 642.
Marble mountain, anorthosites, 579.

: Mountains,

STATE MUSEUM

Marcy, Mt, 51’;
58>.

Mesozoic era, possible history, 621.

Metamorphic rocks, term, 563.

Microperthite, 552, 558.

Miueralogy, 637-648.

Mirror lake, 594.

Moraines, 528, 534, 592-599, 627.

Mountain slopes, configuration, 629.

see Cascade mountain;

Cobble Hill; Eagle Eyrie; Giant;

Gothics; Marble; Pitchoff; Pulpit;

Sentinel; Scotts Cobble.

altitude, 531; peaks,

Norite, 574.

North Elba, boulder at John Brown’s
grave, 597; crystalline limestone, 536;
quartzite, 544.

Orthoclase, 552.

Paleozoic era, possible history, 621.

Pebbles, 599.

Pitchoff mountain, 522; altitude, 531;
eneisses, 567; limestone, 614.

Plagioclase feldspar, 575, 588.

Plains, gravel, 528; sandy, 528, 602.

Porter, Mt, 523; altitude, 531.

Potsdam sandstone, rests on meta-
morphic rocks, 617; boulders, 628.
Pulpit mountain, altitude, 53°; gneiss-

es, 567.
Pyrites, 641.
Pyroxene, 538, 546, 558, 572, 639, 642.
Pyroxene crystals, 542.
Pyrrhotite, 539.

Quartz, 539, 551, 558, 642.

Quartzite, 534, 615; cliffs, 547; distri-
bution and characteristics, 544-549;
age, 609. ‘

Quaternary period, probable history,
627.

Red Rocks, quartzite, 544.

Rivers, courses how determined, 62°.

Rocks, characteristics, 571; geologic
age of, 604-637; varieties, 53°.

INDEX TO MUSEUM BULLETIN 21 67

Sand plains, 528, 63°.

Sands, 592; incoherent, 534; water-
sorted, 599-603,

Sandstone, see Potsdam sandstone.

Saranac, topography, 52°.

Scapolite, 546.

Scotts Cobble, granite, 551.

Sentinel mountain, 521; altitude, 531;
anorthosites, 584; glacial amphithea-
ters, 632; gneisses, 567; quaternary
period, 628; trap dike, 589.

Sunrise Notch, gneisses, 567.

Terraces, fanshaped, 599.

Tertiary period, possible history, 621.

Titanite, 642.

Trap dikes, 534, 553; age, 6185 distri-
bution and characteristics, 585-59! ;
geologic age of, 604.

Utica slate, 619.

Vesuvianite, 641,

Walcott, C: D., acknowledgments to,
512.

Water-sorted sands and gravels, 599-
603.

West Branch, see Ausable river, west
branch.

Weston mine, Keene, 647.

Whiteface Inn, anorthosites, 584.

Whiteface, Mt, 518; altitude, 531;
anorthosites, 578; glacial amphi-
theaters, 631; granite, 549; quater-
nary period, 628.

Wilmington, anorthosites, 579.

Wilmington Notch, 521; granite, 549;
trap dike, 589.

Wilmington valley, anorthosites, 584.

Wilmington village, altitude, 529.

Zircon, 558, 641.

ae.

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