UNIVERSITY OF MICHIGAN
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CGEOLOGIOAL SURVEY BRANCH ' ' 4 M ‘ ‘
Hon. W. TEMPLEMAN, MINISTER; A. P. Low," DEPUTY .Mlmswnm; i
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GEOLOGY
OF AN-
‘ :AREAADJmNmG “THE X EAST SIDE
OF-
‘ 4' LAKE TIMISKAMING
, ‘ ‘ ' QUEBEC ‘ § ’
BY
MORLEY E. WILSON. » * ~ ‘ 1,


v QTTAWA' _
GOVERNMENT PRINTING BUREAU
< 1910
No, 1064 '


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CANADA
DEPARTMENT OF MINES
GEOLOGICAL SURVEY BRANCH
Hone W. TEMPLEMAN, MINISTER; A. P. Low, DEPUTY MINISTER;
R. W. BROOK, DIRECTOR

GEOLOGY
OF AN
AREA ADJOJNING THE EAST SIDE
OF
LAKE TIMISKAMING
QUEBEC
BY
MORLEY E. WILSON.


OTTAWA
GOVERNMENT PRINTING BUREAU
1 9 10
6487—1 No. 1064
To B. W. BROOK,
Director Geological Survey,
Department of Mines.
SIR,-——I herewith beg to submit a report on the geology of an area
adjoining the east side of Lake Timiskaming, to be accompanied by
a geological map of the Lake Timiskaming Mining Region.
I have the honour to be, sir,
Your obedient servant,
(Signed) MORLEY E. WILSON-
OTTAWA, May 19, 1908.
6487—— I}
CONTENTS.
Page.
Introduction.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 7
Physical features. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 8
Geology.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 10
Keewatin.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 13
Metamorphosed greenstones.. .. .. .. .. .. .. .. .. .. .. .. 13
Iron formation rocks.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 17
Quartz porphyrite.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 18
Laurentian.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 20
Granite and gneiss.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 20
Huronian.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 25
Conglomerate and greywacke.. .. .. .. .. .. .. .. .. .. .. .. 28
Quartzite, arkose, and conglomerace.. .. .. .. .. .. .. .. 30
Origin of the Huronian rocks.. .. .. .. .. .. .. .. .. .. .. 31
Diabase and gabbro.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 32
Silurian.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 36
Clinton and Niagara.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 36
P1eistocene.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 37
Economic geology.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 37
Gold.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 37
Silver.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 37
Copper.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 40
Iron.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 40
Asbestos.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 40
Limestone.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 40
Clay.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 41
Index.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 43
ILLUSTRATIONS.
. Page.
Plate I. Third Rapid, Riviere des Quinze.. .. .. .. ..Frontspiece
Burnt Island Rapid, Riviere des Quinze.. “
Plate II. Glacial erratic of Laurenian gneiss, 'near Ot-ter 1ake.. .. .. 20
Plate III. Fig. 1. Granite associated with gneiss from Shingwak lake. 22
Fig. 2. Altered feldspar enclosed in fresh quartz and ortho-
clase, Lac des Quinze.. .. .. . .. .. .. .. 22
Plate IV. Fig. 1. Feldspathic quartzite near Otter Lake.. .. .. .. .. 30
Fig. 2. Reaction rims in olivine diabase, Blueberry island,
Lake Kipawa.. .. .. .. .. .. .. .. .. .. .. .. .. 30
Plate V. Fig. 1. Diabase near Fabre wharf.. .. .. .. .. .. .. .. .. 34
Fig. 2. Intergrowth of feldspars in diabase, Fabre township. 34
Plate VI. Contact of Silurian limestone and Huronian quartzite, near
Piché point.. .. .. .. .. .. .. .. .. .. .. .. .. .. 36
MAP.
No. 1066. Lake Timiskaming Mining Region.
5
REPORT ON THE GEOLOGY
OF
AN AREA ADJOINING THE EAST SIDE OF LAKE TIMISKAMING, QUE.
BY
MORLEY E. WILSON.
INTRODUCTION.
As stated in the Summary Reports of 1906 and 1907, the
geological examination of the district adjoining the east side of
Lake Timiskaming was undertaken for the purpose of determining
the extent easterly of those geological formations which in Ontario
have been found to contain cobalt-silver-nickel ores, and of delimit- '
ing the various geological boundaries in greater detail than had
hitherto been attempted. ‘
The present report, with the accompanying geological map, repre-
sents the result of two seasons’ ﬁeld-work, viz., that of 1906, and 1907.
During 1906 the ﬁeld operations were under the direction of Dr.
A. E. Barlow, but owing to his absence from the ﬁeld during a great
part of the summer, and his subsequent retirement from the staﬁ of
the Survey, the work devolved upon the writer as his assistant. The
area examined comprises about 600 square miles, extending from
Lake Timiskaming to Lake Kipawa and Lac des Quinze, and from
Riviere des Quinze to the south end of Fabre township.
1n the preparation of the map, surveys were made of roads, trails,
creeks, lakes, etc., using the Rochon micrometer and surveyor’s com-
pass. These, while necessary adjuncts for a correct topographical
map, were also utilized for locating geological boundaries. In those
portions of the area surveyed into townships the lot posts, which
occur on the range lines at intervals of thirteen chains, were em—
ployed for the same purpose.
Geological descriptions of parts of the area have appeared from time
to time in the publications of the Geological Survey. In 1845, Sir
Wm. Logan undertook the examination of the Ottawa river, continuing
7
8 GEOLOGICAL SURVEY, CANADA
his investigations as far as the third rapid on Riviére des Quinze.
His report contains a brief outline of the geology of the east side of
Lake Timiskaming.1 In 1872, Mr. Walter McOuat was engaged in
making a geological examination of a ‘ portion of the country on
the Ottawa to the northward and eastward of Lake Timiskaming.’
This undertaking included an [examination of Riviere and Lac des
Quinze, the geology of which is very accurately described in the
report of his ﬁeld-work for that season.2 A detailed account of the
geology of Lake Timiskaming, and Riviere des Quinze, together
with an appendix by Dr. Ami on the fossils of the Silurian outlier
of the Timiskaming district, is given by Dr. Barlow in his report
on the geology and natural resources of the area included in his
Nipissing and Timiskaming map sheets. This report, which was a
resumé of observations extending through several seasons, was pub-
lished in 1897 .3
Prof. Miller’s report on the cobalt-nickel arsenides and silver
deposits of Timiskaming, issued in 1905, contains several references
to the geology of the east shore of Lake Timiskaming, and more
particularly to the deposit of argentiferous galena occurring- at
Wright mines.4
In the report of the Department of Mines of Quebec, for 1906,
Mr. Obalski mentions the mining developments being carried on in
this region, which he had visited during the previous summer in the
course of a reconnaissance through the western part of Pontiac
county.5
Physical Features.
The topography of the country east of Lake Timiskaming, while
possessing in part those characteristics common to the Archaean
peneplain, has been greatly modiﬁed by extensive deposits of post-
glacial materials. These consist largely of stratiﬁed clays, which
have ﬁlled in the depressions in the uneven rocky surface, producing
ﬂat, almost plain-like areas, which diﬂer strikingly from the more
rocky portions of the district. It is probable that many of the
higher rock exposures, which project through the clay as knobs,

1Report of Progress, Geo. Surv. Can., 1845-6.
2 Report of Progress, Geo. Sur. Can., 1872-3.
3 Annual Report, Geo. Surv. Can., Vol. X.
‘Reoort of Bureau of Mlncs, Pt. 2, 1905.
5 Report of Department of Mines, Que, 1906.
EAST SIDE OF LAKE TIMISKALUNG, QUE. 9
‘hills, or ridges, played the part of islands in the huge post-glacial
lake which covered the northern part of the Timiskaming area, and
from which the bedded clays were laid down.
Of the physical features which distinguish the rocky areas from
those in which clay predominates, the most prominent are those
associated with the hydrography of the region. In the former areas
lakes are abundant, while in the latter they seldom occur; and the
streams, which in the rocky areas are rapid and without deﬁnite
channels, in the clay areas meander slowly between high banks of
stratiﬁed clay. With the exception of the Galt-St. Amant-Morin
chain of lakes, which have their outlet into Lake Kipawa, the
drainage of the region is almost exclusively into Lake Timiskaming;
and that the above series of lakes ﬂow into Lake Kipawa is not due
so much to the general slope of the surface as to the way in which
the drift has obstructed the long, narrow depressions in which they
occur. The greater part of the drainage into Lake Timiskaming is
by way of the Otter river, the remainder being distributed between
Little river, Young and Lavallée creeks. All of these have their
sources in the interior lake country, passing through the clay ﬂats
in the lower part of their course.
Although the surface of the country on the whole is somewhat
rugged, yet, as is generally found throughout the Archaean plateau,
extreme diﬁerences of elevation do not occur, a hill rising over 200
feet above the surrounding country being a somewhat striking topo-
graphical feature. The most prominent elevations in the district
are 1a series of hills and ridges which parallel the east side of
Lake Timiskaming from Lavallée bay to Apika creek. These,
while not having an altitude of more than 400 feet above the lake,
are rendered very conspicuous by contact with the ﬂat clay areas
enclosing them. The interior rocky areas have either the monoto-
nous, mammillated surface characteristic of the glaciated granite
and gneiss, 'or the still more pronounced low relief of the Keewatin.
The highest elevation in the whole area occurs a short distance
north of Lavallée lake, the altitude being nearly 1,200 feet above sea-
level, or 600 feet above the level of Lake Timiskaming.
The close relationship between the topography and the under-
lying geological conditions, which have been frequently noted as
characteristic of the Archaean, is well exempliﬁed in this region.
The low relief of the Keewatin, the monotonous roche moutonne
surface of the granite and gneiss, the low clay covered areas of
10 GEOLOGICAL SURVEY, CANADA
greywacké, and the abrupt rocky hills of quartzite have each their
own typical surface features, which are directly related to the nature
and structure of the rocks themselves. Lakes, which occur in
massive rocks having no lines of weakness along which decay and
erosion could act, possess irregular outlines, while those which occur
in schists or gneisses have elongated trough-like basins, correspond-
ing in direction to the foliation of the enclosing rock.
There are, however, a number of lake basins which have no
apparent relationship to geological conditions. This is best exem-
pliﬁed by those which occupy the long rocky depressions extending
from Galt to Otter lake. This valley, while on a much more limited
scale, is precisely similar to that of Lake Timiskaming in direction
and general character, and probably resulted from the same cause,
or set of causes, to which the latter owes its origin. The remarkable
parallelism in the watercourses of the Timiskaming area has been
noted by Prof. Miller,1 which, he supposes, has been brought about
by regional disturbances in post-middle Huronian times. The very
ancient, probably pre-Palaeozoic existence of the Timiskaming valley,
is proved by the Silurian outlier which occurs at the north end of
the lake, and, while the attitude of the rocks both on Timiskaming
and on the Galt-Otter series of lakes seems to prove that these
depressions are not due to folding, their linear and parallel character
would suggest that extensive faulting had possibly determined their
direction. But whether they originated primarily from regional
movements or not, the latter alone would not be sufﬁcient to account
for the existence of such deep rocky gorges. It would, therefore,
seem more prob’able that aqueous erosion has played the important
part in giving these parallel depressions—of which the Timiskaming
caﬁon is the most conspicuous member—their present physiographic
character.
Geology.
The geology of the district diﬁers but slightly from that described
elsewhere in the Timagami-Timiskaming area, presenting rocks of
the same varieties, and in the same stratigraphical relationship. The
various formations, with their equivalents, as found on the Ontario
side of Lake Timiskaming, are as follows :—

1 Report of Ontario Bureau of Mines, Part II, 1905.
EAST SIDE OF LAKE TIMISKAMING, QUE. 11
QUEBEC. ONTARIO.
Prers'roosnm. PLEISTOCENE.
P'ost-gllalcial— Postagljacial—
Stratiﬁed clay and sand. Stratiﬁed clay and sand.
Glacial— Ghacial—
Gravel, sand and Iboulder clay. Gravel, sand and boulder clay.
Unconfo'rmzty. Unconformz'ty.
PALAEOZOIC. PALAEOZOIC.
Slilulrian— Silurian—
Clinton and Niagara limestone,
Clinton and Niagara limestone,
sandstone and conglomerate.
sandstone and conglomerate.
Unconfo'rmity. Unconformity.
PIKE-CAMBRIAN. PRE—CAMBRIAN.
Hu r-onian— Huron'i'an, middle—-
Conglomerate. Lorrain arkose,
Quartzite and arkose..
No apparent unconjo'r'mzty.
quartzite _and conglomerate.
Unconformzty.
Hurontan, lower——
Cobalt series :
Greywacké. Greywacké, quartzite,
Conglomerate. conglomerate, etc.
Unconformity.
Keewatin— Unconfo'rmity.
Quartz-Ip’onphy-ri-‘te. Keewatin—
Iron formation. Quar-tz-porphyries, greenstone,
Serpentine, hornblende-schist, etc. '
diabase.
INTRUSIVES. INTRUSIVES. __
Post-Huronian—
Diabase and gab‘bro.
Post-Keewatin—
Gr-anrite.
Post-Huronrian—
Die-base and gabbro. s
Granite.
Post-Keewatin—
Granite and gneiss.
It will be observed that the Huronian here diﬁers from that of
the Cobalt area in the absence of any evidence of unconformity
between the conglomerate and greywacké, and the overlying quart-
zite and arkose. The presence of a post—Huronian acid intrusive, as
far as known, is also a distinguishing feature. But in other respects
the two areas, from a geological standpoint, are practically identical.
There are, however, some differences in the extent of the members
comprising the various formations. Thus, while on the Quebec side
of the lake quartz—porphyry,1 or porphyrite, is an important Kee-
watin rock, on the Ontario side this occurs only in dikes; but in the
case of the post-Huronian diabase, the conditions are reversed, these
rocks being very prominent in Ontario, and of minor extent in
Quebec.
The early history of the pre-Cambrian of the district, of which
there is a distinct record, is largely that of a succession of igneous

1 Report of Bureau of Mines, Pt. II, p. 42, 1905.
12 GEOLOGICAL SURVE Y, CANADA
intrusions, with accompanying dynamic action, which resulted in the
formation of schists and other metamorphic rocks. The oldest
members of this complex consist of metamorphosed diabase, and re-
lated eruptives. Interfolded with these are jaspery or quartzose
magnetite bands, which represent a sedimentary phase of the period.
The eruption of the greenstones, and deposition of the iron forma-
tion beds, was followed by an extended intrusion of quartz porphyrite,
dikes of which penetrated the older greenstones and iron formation
rocks. It is thus possible to distinguish three divisions in the igne-
ous-sedimentary series of rocks just described, although in the case
of the older greenstones others no doubt exist. These rocks, which
comprise the Keewatin formation, have been cut by a coarse biotite
granite belonging to the Laurentian in age.
The intrusion of the Laurentian was followed by a long period
of quiescence from eruptive activity, during which epigene forces
were in active operation. The ordinary present day processes of
erosion and decay were doubtless at work on the Keewatin-Lauren-
tian rock surface at this time, the long-continued action of these
destructive agencies resulting in the accumulation of large quanti-
ties of fragmental materials. The Huronian rocks were then de-
posited on this uneven and weathered ﬂoor in the general sequence,
conglomerate, greywacké, quartzite, conglomerate, all in apparent
conformable succession. ‘
The formation of the Huronian clastics was followed by two
successive igneous intrusions, the ﬁrst of which consists of granite
and the second of diabase, the latter being the equivalent of the
rocks with which the silver-cobalt ores Of Ontario are associated.
The post-Huronian intrusion concluded, as far as can be
recognized, eruptive activity in the area; but widespread oscil-
lations of a continental type, as well as more local differential
movements, have occurred since that time. The climax of a down—
ward movement was reached in the Palaeozoic period when the whole
area was submerged and a great thickness of sediments deposited,
a remnant of which remains in the Silurian syncline of the north
end of Lake Timiskaming. The denudation which took place prior
to the transgression of the Palaaozoic ocean was so tremendous that
it is difﬁcult to form an adequate estimate of the time which must
have elapsed. It was sufﬁcient for the carving down of an uneven,
possibly mountainous country to the condition of a peneplain, and
EAST SIDE OF LAKE TIMISKAMING, QUE. 13
for the further erosion of such rocky excavations as the Timiska-
ming caﬁon, 1,000 feet deep.
On the retreat of the Palaeozoic ocean, and the return to con-
tinental conditions, the work of surface degradation was resumed,
and continued without interruption up to the time of the glacial
epoch. The disintegrated materials accumulated during this long
interval of decay were then swept from the surface by the advancing
ice sheet, leaving it in the uneven, mammillated condition character-
istic of the rocky portions of the region. On the retreat of the
glacier the debris acquired during the more aggressive periods of its
history was left behind, scattered over the rocky ﬂoor as gravel, sand
and till. A large fresh-water lake then covered all the lower areas
of the region, depositing the ﬂats of stratiﬁed clay so prominent in
the district. The deposition of these post-glacial clays concluded in
the main the geological history of the area, the processes of erosion
and decay having effected little change since that time.
Keewatin.
METAMORPHOSED GREENSTONES.
The oldest and most extensive subdivision of the Keewatin forma-
tion is an igneous complex of a number of altered intermediate to
basic rocks, the exact original nature of which cannot always be
determined, but to which the general name metamorphosed green-
stones is applicable. They resemble one another in that they are all
green in colour, have been greatly metamorphosed, are igneous in
origin, and belong to the same very ancient period of eruptive
activity, though they are not all of exactly the same age, since they
are sometimes observed to cut one another. .
These greenstones are found in ﬁve localities, which may be
deﬁned as the Baby, Duhamel, Rousselot Lake, Lac Clair, and Fabre
areas.
The Baby greenstone consists in reality of two portions. The
smaller one, occurring in the southern part of ranges IV and V, is
cut off from the larger area by intruded quartz-porphyrite. This
main area, which occupies nearly the whole of the northern part of
the township, has its southern limit marked out by the quartz-
porphyrite, the contact with which extends from the south end of
Cameron lake to a point north of Kirwan lake, then southward
around the south end of Long lake. On its western border the'
14 GEOLOGICAL SURVEY, CANADA
greenstone disappears beneath the clay, so that its extent in this
direction can only be approximately determined from isolated ex-
posures along the watercourses, where erosion has removed the
overlying Pleistocene materials. The most westerly outcrops of the
rock occur at a chute on Cameron creek, on lot 35, range VIII,
Guigues, and on Riviere des Quinze from lot 57, range IX, of the same
township. Ascending Riviere des Quinze, on lot 57, range IX, Guigues,
the greenstones continue until the Maple rapids are reached, where
they are followed by a gneissoid granite. The dividing line between
the two rocks occurs on the north shore immediately above the
rapids, from which point it crosses the river obliquely to the south-
east, and maintains this direction for nearly a mile, when it turns
southward, passing about midway between Long and Warne lakes.
How far the Baby greenstone extends northward beyond Riviere des
Quinze was not ascertained, being beyond the limit of our investiga-
tions.
The greenstone of Duhamel township consists entirely of a mass
of serpentine rock, almost completely buried beneath the clay, and
appearing on the surface merely as a succession of four small ex- '
posures, extending from lot 15 to lot 29, range VII.
The third greenstone area parallels the north shore of Rousselot
lake. It may be roughly deﬁned as extending, in a north and south
direction, from lot 33 to lot 36, and in an easterly and westerly
direction, from range III, to range VII, Laverlochére township. Two
very small exposures of greenstone occur on lots 37 and 38, range VII,
Laverlochere, which probably belong to the same rock mass, though
the rock is not exposed in the intervening distance.
In the vicinity of Lac Clair, on range XIII of Laverlo-
chere, the greenstone appears again. The rock here occurs in a
belt nearly one and a quarter miles in width, extending eastward
beyond the limits of the area examined. The southern border of the
band skirts the north shore of Little Otter lake.
An area of Keewatin rocks occupies the central portions of lots
7, 8, 9 and 10, range VII, Fabre, the northern part of which is com-
posed of the more basic member of the series—the greenstone, and
the southern part of the acid type of eruptive—the porphyrite.
Mining development work has been carried on here for the last two
years, by the Jessie Fraser Copper Mining Company, the property
being known locally as the Mitchell mine.
EAST SIDE 0E LAKE TIMISKAMING, QUE. 15
The greater part of the rocks comprising the metamorphosed
greenstones have not only undergone the ordinary alterations which
must necessarily have taken place in rocks of such antiquity, but
have also undergone structural changes resulting from the mechani-
cal stresses to which they have been subjected. Hence, while massive
types of the rock sometimes occur, they more frequently show at
least some trace of foliation. A peculiar variation in the green-
stone was observed on the north shore of Riviere des Quinze, at the
foot of the Cypress rapids. Large, augen-like aggregates of feldspars,
showing a rough parallelism in their elongation, occur enclosed in a
ﬁne-grained, ophitic groundmass. The occurrence of this rock was
observed by Mr. McOuat, whoadescribes it as follows: ‘There are
also in many places numerous obscure lenticular masses of a felds-
pathic character, . . . . showing crystals of feldspar, and usually
ﬂakes and streaks of a dark green hornblende. The latter, as well
as the whole mass, which may be from an inch to several feet long,
and from a line to several inches in thickness, are parallel with the
general bedding (foliation) of the rock.’ Uralitic diabase or gabbro
and hornblende schist, with a series of rocks of an intermediate type,
comprise the mass of the greenstones. Serpentine rocks also occur
to a limited extent.
The last-mentioned rock was observed to comprise ﬁve rock ex-
posures, four of which form the Duhamel greenstone area, and the
ﬁfth a small, rocky point on the north shore of Rousselot lake. In
the ﬁrst locality the rock is a soft, dark-green, massive variety,
which, under the microscope, is seen to be made up of ﬁbrous ser-
pentine through which is disseminated fragmental and dusty magne-
tite. In the second locality the serpentine is a light-green, granular
rock, which, when microscopically examined, was found to consist of
serpentine, magnetite, ilmenite, and leucoxene, the whole traversed
by veinlets of calcite.
The diabase-gabbro-hornblende schist series of greenstones, which
comprise the mass of the Keewatin basic eruptives, examined in
section show very distinctly the successive stages in the paramorphic
and metasomatic metamorphism to which the rocks have been sub-
jected. The ﬁrst step in the transformation of the rock is the
alteration of the pyroxene to a strongly pleochroic hornblende, and
of the plagioclase to saussurite. As the process of degradation con-
tinues, the hornblende becomes ﬁbrous, frayed out at the margin,
and altered to chlorite, while the alteration of the plagioclase
16 GEOLOGICAL SURVEY, CANADA
becomes so complete that even the outline of the original feldspar
disappears, the presence of epidote, sericite, and other decomposition
products being the sole evidence of its former existence in the rock.
Very often the plagioclase is fractured and broken, especially in
those localities where dynamic action has been most intense.
Secondary quartz and feldspar, calcite, pyrite, and ilmenite—the
latter frequently enclosed in a border of leucoxene—are the other con-
stituents most frequently observed in the rock. In those greenstones
possessing a distinctly schistose structure an almost-complete re-
crystallization appears to have taken place. The hornblende occurs
in well deﬁned rod-like fragments showing a distinctly parallel
arrangement, the remainder of the section being ﬁlled with inter-
locking grains of secondary quartz, slightly elongated in the direc-
tion of parallelism. A few scattered fragments of magnetite occur
in the section, being the only other mineral usually present.
The transition, which can be observed both microscopically and
in the ﬁeld between the more massive greenstones and the schists,
leaves little doubt but that originally the two rocks were identical,
consisting largely of diabase, with possibly some gabbro. While no
doubt the metamorphism of the diabase was in part of a regional
type, the close association of the schists with the borders of the
intruded acidic rocks would indicate that contact action was an
important transforming agency. Not only do the schistose rocks
adjoin the intrusives, but the direction of their foliation is parallel
to their margin. This is best exempliﬁed along the greenstone—
granite contact east of Long lake and above the Maple rapids on
Riviere des Quinze.
The few small areas of serpentine which occur in the district
appear to form quite a distinct rock from the other Keewatin basic
eruptives. Their correlation with the greenstones is largely a matter
of analogy, since they were never observed in actual contact with
one another. Their metamorphosed character, however, together
with the fact that similar rocks occur associated with the Keewatin
schists in other localities, seemed to be suﬁicient basis for their
classiﬁcation with the Keewatin greenstones, though in what rela-
tionship to the other members of the group was not ascertained. The
alteration which has taken place in the rock has been so complete
that little evidence was obtained as to its original nature from its
microscopic examination.
EAST SIDE OF LAKE TIMISKAMING, QUE. 17
The Keew-atin greenstones of the area are to a large extent
intrusive, or if volcanic, they at least cooled under great pressure.
They do not show any of the characteristics of eifusive rocks, unless
the occurrence of an ellipsoidal schistosity is to be considered as
such. This feature resembles in some respects the ellipsoidal struc-
ture described in the Vermilion district of Minnesota, but differs
from it in being less pronounced and much more regular. The
structure is best shown in the Lac Clair greenstone area, the regular
succession of ellipsoids giving the weathered surface a net—like
appearance. It was also observed in the same locality, that the
longer axes of the ellipsoids were parallel to the strike of the neigh-
bouring iron formation. This peculiar foliation, unlike that of the
Vermilion district, would appear most probably to have originated
from the application of pressure to a rock possessing a columnar
structure, though the shearing- of a regularly jointed rock might
produce the same result.
IRON FORMATION ROCKS.
The iron formation rocks of this region include two types of a
somewhat different character, consisting of magnetite or siliceous
magnetite, interbanded in one case with quartz and in the other with
jasper (jaspilite). The former variety occurs in the vicinity of Lac
Clair, and the latter crossing the portage from Riviere des Quinze
to Kakake lake. Both of these ranges have a nearly vertical dip,
and a strike corresponding to the foliation of the including green-
stones.
The iron formation which occurs enfolded in the Lac Clair green-
stone area consists of a number of outcrops, a few feet in length,
appearing on the surface at intervals for a distance of over two
miles. The maximum width of the exposure is about 30 feet, and
the general strike N. 96° E. These iron-bearing rocks are very
siliceous, and contain a considerable amount of iron pyrites. They
have been greatly faulted and are cut by porphyry dikes. It is
probable that the large quantities of iron oxide being deposited on
the pebbles and boulders on the shores of Little Otter lake have been
derived from this source.
The Kakake Lake jaspilite, being located on the portage route
which follows Riviére des Quinze, was observed by Mr. W. McOuat
when making his geological examination of that river. The following
6487—2
18 GEOLOGICAL SURVEY, OANADA
description of the occurrence is taken from his report :1 ‘ It occurs
in the form of layers, from the thickness of paper to about an inch,
and is interlaminated with similar layers of a whitish, grey and
dull-red ﬁne-grained quartzite. The iron ore constitutes probably
from one-fourth to one—third of the whole, and as the thickness of
the whole band is about thirty feet, the total thickness of the layers
of iron ore would probably not be less than eight feet. The band
was traced along the strike for about one hundred yards.’ The
‘presence of jasper in this locality is due no doubt to slightly
different local conditions, which caused red oxide of iron to be
disseminated through the quartzose bands. The strike of this iron
formation is N. 20° E., and the dip N. 70° E. < 75°.
In the Lac Clair district there are a number of elongated patches
of conglomerate, included in the Keewatin, and which contain
pebbles Of greenstone and banded iron, evidently derived from the
surrounding rocks. The exact geological position of these conglom- '
erates is not at all apparent, though it would seem probable that they
represent remnants Of the basal member Of the Huronian which at
one time overlay the greenstone. This rock is possibly similar to
the ‘ disturbed and squeezed conglomerates intimately related to the
Keewatin,’~ mentioned by Mr. Brock in his report on the Larder
Lake district. There are some quartzite rocks included in the Kee-
watin greenstones which may possibly be of sedimentary origin.
Examples of this occur a short distance south of the Head rapids
on Riviere des Quinze, and on the south shore of the same river
below the Cypress rapids.
QUARTZ PORPHYRITE.
The youngest member of the Keewatin igneous rocks, to which the
name quartz porphyrite has been applied, has its largest extent in
the southern part of Baby, and the adjoining portions of Guigues
township. The rocks in this locality on the whole are but poorly
exposed; more especially is this the case in the western and southern
portions, where they are overlain by the post-glacial stratiﬁed clays.
The northern boundary of the area is deﬁned by the greenstone con-
tact, which extends eastward from the southern end of Cameron
lake. Like the older Keewatin eruptive farther north, it is cut off

1 Report of Progress, Geol. Surv. Can., 1872-73, pp. 131-2.
2 Report of Bureau of Mines, Pt. I, p. 208.
EAST SIDE OF LAKE TIMISKAMING, QUE. 19
on the east by granite, the junction occurring about one mile east
of Robinson lake. The southern border of the porphyrite area, with
the exception of the portion in ranges IV and V, Baby, which is inter-
cepted by greenstone, is also in contact with granite. The junction
between the porphyrite and greenstone occurs on lot 9, range IV, from
which point the area of porphyrite extends southward, the most
southerly exposure in Baby township being situated on lot 4, range III.
There are no outcrops of granite or porphyrite in close proximity
to one another in range II, Baby, but the dividing line between the
two rocks probably occurs on lot 6, continuing westward across
range I into Guigues township. A southerly extension of the porphy-
rite here occurs, reaching to lot 58, ranges VI and VII, Duhamel.
The rock is not sufﬁciently exposed for its western border to be
delimited, but its most westerly exposure occurs on the Otter river,
on lot 13, range VII, Guigues.
Two other small areas of porphyrite were observed in the region,
one of which occurs on lots 7, 8 and 9, range VII north, Fabre,
comprising the southern part of the Mitchell mine, Keewatin area.
The second of these areas is found on lots 7 and 8, range V south
of the same township.
The Keewatin quartz porphyrite, unlike the older greenstones,
has not been subjected to great mechanical deformation, although
minerals of a secondary type have been abundantly developed in
the rock. Macroscopically the porphyrite is usually variegated in
colour and decidedly porphyritic. Blebs of blue quartz are dis-
tinctively characteristic of the rock wherever it occurs.
Examined under the microscope the quartz-porphyrite is found
to consist of phenocrysts of quartz and plagioclase enclosed in a
cryptocrystalline groundmass of-which quartz and feldspar are the
most prominent constituents, but also containing epidote, calcite,
chlorite and other minerals. Determinations of the extinction
angle, in sections at right angles to the brachy-pinacoid, show the
plagioclase to be largely labradorite. A few crystals possess a
zonal structure, as indicated by zonal extinction under crossed
nicols. An abundance of microlitic inclusions of epidote and mus-
covite occurs disseminated through the feldspars, apparently the
result of their incipient decomposition. The crystals of plagioclase
are distinctly idiomorphic, though somewhat corroded on their
margin; those of quartz are rounded and granular on the edge, with
embayments, of the groundmass running into them. The quartz is
6487—2}
20 CEOLOGlCAL SURVEY, CANADA
frequently broken, the fracture being ﬁlled with calcite and epidote.
Aggregates of epidote, associated with chlorite, frequently occur in
the section, suggesting the former presence in the rock of some ferro-
magnesian mineral. Ilmenite and leucoxene are occasionally ob-
served to be present. ‘
Along the borders of the quartz-porphyrite areas we sometimes
ﬁnd dikes penetrating the adjoining greenstones, which, while not
porphyritic when examined microscopically, are found to be precisely
similar to the groundmass of the porphyrite. In the absence of the
structures characteristic of effusive rocks, it. would thus seem prob—
able that the quartz-porphyrite is intrusive, and that the large areas
of the rock represent sills or laccolites rather than surface ﬂows.
LAURENTIAN.
GRANITE AND GNEISS.
The acid igneous rocks, granite and gneiss, comprise nearly the
whole of the eastern and southern _portions of the area mapped.
Commencing below the Head rapids on Riviere des Quinze, the
western border of these rocks extends southeasterly for nearly a mile,
then turns southward, passing from nearly midway between Long
and Warne lakes to the eastern extremity of range V, Baby town—
ship. Between this point and Otter lake a westerly extension of granite
occurs, occupying the whole of northern Laverlochére and reaching
to range IV of Duhamel, where it disappears beneath the quartzite
and arkose. It again emerges, however, on the shores of Baic
des Peres in two small areas. From Otter lake the border extends
in an almost straight southeasterly direction to lot 18, range I, Fabre.
With the exception of the Lac Clair Keewatin area, and occasional
dikes of intermediate to basic rocks, all the district to the east of
this limit consists of granite and gneiss.
The rocks included in the area just outlined, however, are not all
of the same age, as shown by their relationship to the Huronian.
Several contacts, which have been described below, occur in Duhamel,
northern Laverlochere and Fabre, where the granite is unconformably
overlain by conglomerate or arkose. But in contrast with this, a con-
tact was observed about two and a half miles southwest of Otter lake,
where the granite is intruded into the Huronian. The Huronian is
represented at the point of juncture by greywacké, large masses of
which are included in the granite in the vicinity of the contact.
PLATE II.


7
Ian gneiss
I
lCO
0
Glacia
near Otter Lake.
f Laurent
l errat
p. 20
6487
EAST SIDE 0E LAKE TIMISKAMING, QUE. 21
The dividing line between the two rocks is fairly deﬁnite, the granite
sending off small stringers into the greywacké along its margin. It
may also be noted in this connexion that small areas of conglo-
merate occur, surrounded by the granite near its contact with the
I-Iuronian, east of Otter lake. While these may be remnants of a
conglomerate laid down on the granite, in view of the relationship
which exists farther west, it would seem more probable that they
had been included in the granite by its intrusion.
We thus have in this area acid igneous intrusives of two ages,
one of which, the post-Keewatin, is younger than the Keewatin, but
antedates the Huronian, while the second, the post-Huronian, is
younger than both the Keewatin and Huronian. In the absence of
overlying Huronian it is not possible to distinguish the two varieties
of the rock with sufﬁcient certainty for mapping purposes; but Since
the granite which cuts the Huronian passes into and is apparently
continuous with the banded gneiss which occurs so extensively in
the southeastern part of the area mapped, it may be possible that all
of this rock should be classed as post-Huronian. If this assumption
were correct, the gneissic rocks, usually called Laurentian, in this
area at least, would be of later age than the Huronian. For the
purpose of petrographical description the granite found in Duhamel,
northern Laverlochere, and southern Fabre, which is undoubtedly pre-
Huronian in age, has been separated from the remaining areas of
acid intrusives in which the banded gneiss predominates.
The rock belonging to the ﬁrst class is a massive granite, usually
coarse, sometimes porphyritic in texture, varying in colour from red
to grey according to that of the feldspar, its dominant constituent.
As found on the shores of Baie des Peres, this rock is a coarse, red
variety, identical with the Lorrain granite—so designated by Pro-
fessor Miller—which occurs directly opposite on the Ontario side of
Lake Timiskaming. A ridge of granite porphyry extends along the
line between ranges I and II, Laverlochere, from lot 30 to lot 38,
which contains large pink crystals of orthoclase up to an inch in
length, but elsewhere throughout this township the rock is a grey
uniformly textured type. In southern Fabre it is ﬁner grained and
slightly gneissoid.
Examined in section, this rock is generally found to be a biotite
granite, though hornblende is occasionally present. The feldspars
consist of orthoclase, microcline and acid plagioclases, the micro-
cline being usually the more abundant. The plagioclase is often
22 GEOLOGICAL SURVEY, CANADA
clouded and altered to sericite and epidote. The biotite is never
abundant, and is usually in the last stages of alteration to chlorite.
Hornblende, when present, occurs in strongly pleochroic, idiomorphic
individuals, which are also sometimes greatly chloritized. Calcite,
scattered grains of magnetite, and wedge-shaped fragments of
titanite, are frequently found in the section. The quartz is usually
pink, slightly fractured and allotriomorphic. The microcline is much
fresher than the other feldspars, and is evidently of secondary origin.
The prevailing rock in the second division of acid intrusives is
a banded biotite or hornblende gneiss, but with which are associated
areas of homogeneous granite, or gneissoid granite, varying in extent
from a few feet to several miles. The alternating bands, which are
sometimes deﬁnite, but more frequently merge into one another, are
distinguished by variations in colour and composition, arising from
differences in either the quantity or variety of their constituent
minerals. They also vary in texture, sometimes consisting of peg—
matite, or possessing lenticular feldspathic inclusions. Bands of
hornblende gneiss up to several inches in width may alternate with
those in which biotite is the dominating bisilicate; or bands in
which biotite or hornblende are abundant may alternate with those
_ in which lesser quantities of these minerals are present. The banded
gneisses are sometimes interrupted abruptly by local areas of rock,
consisting of granite similar in mineralogical composition to the
bands, but cutting one another irregularly. At such points ball—like
segregations of very basic gneiss a foot or more in diameter occa-
sionally occur. In these areas, where the banded gneisses are re-
placed by a uniform gneiss or granite, the ferromagnesian constitu-
ents are usually found in aggregates, the foliation shown by the rock
being due to a parallel arrangement of these nuclei. The strike and
dip of the gneissic rocks are in general remarkably uniform, though
many minor variations occur, the banded gneisses more especially
being folded locally into dome-like and other plicated forms. The
general direction of foliation is northeasterly, except in the vicinity
of the upper part of Lac des Quinze, where it becomes northerly.
Of the division of acid intrusives which are largely foliated, the
portions consisting of the banded type of gneiss are conﬁned to
either the southeastern part of the area or to the neighbourhood of
the upper part of Lac des Quinze. Elsewhere the rock is either a
uniform gneiss or a granite. It may be noted in attempting to point
out the distribution of the varieties of these gneissic rocks, that
.wm x TNEQGHEQQ 32H .EmﬁoozﬁO was 5.5:@ :12“ E 1.1225 .Emmgwrm ww.$:<|.m .mi


é: mane A;
.wm x a.er xeismcEw 25.: memesw :33 wouﬁeomwe mﬁcgwlé .mfm
6487-Tp. 22
EAST SIDE OF LAKE TIMISKAMING, QUE. 23
there usually appears to be a transition from banded gneiss through
the unbanded type to massive granite, whenever it occurs adjoining
the Keewatin formations.
When examined microscopically these rocks are generally found
to conform in mineralogical composition to some variety of granite
~or its foliated equivalent gneiss, although in a few localities the
hornblendic varieties are found to approach that of a syenite, or
even that of a diorite. The chief minerals present in the rock, in
addition to quartz and feldspar, are biotite, epidote, hornblende and
muscovite, the particular variety of granite or gneiss being deter-
mined by the relative abundance of one or more of these constitu-
ents.
By far the most widespread type of rock comprising these acid
intrusives may be described as a biotite granite or gneiss. Examined
microscopically, the rock is found to contain an abundance of quartz,
usually fresh and free from inclusions, and often forming a mosaic
of interlocking grains. Sometimes a whole section is largely made
up of such a mosaic of quartz and feldspar, while at other times large
feldspar aggregates, usually in various stages of decomposition, are
enclosed in a matrix of fresh granular quartz or of quartz and feld-
spar. Micropogmatitic intergrowths of quartz and orthoclase some—
times occur in sections of this granular type.
In those feldspars in which decomposition has set in, the altera-
tion products are found to consist of sericite and epidote, the trans-
formation usually proceeding along the cleavage lines. Orthoclase
is the dominating feldspar, although the more acid plagioclases
frequently occur. Microcline is often present, and appears to replace
the orthoclase where dynamic action has been more intense. The
biotite present in the rock occurs, as a rule. in elongated, strongly
pleochroic fragments, usually fresh but sometimes altered, either
completely or in part, to ﬁbrous, green chlorite. In addition to the
biotite the mineral epidote is generally prominent, not only as a
decomposition product, but also as an original constituent of the
rock. It usually occurs in well deﬁned fresh, pleochroic, idiomorphic
fragments, associated with and sometimes completely enclosed in
biotite. In many sections cavities in the mineral, as well as inlets
along its border, have been ﬁlled with quartz. Cleavage parallel,
001 (OP), while not frequent, as a rule, is very distinctly Shown in
the epidote individuals. Kernel-like or wedge—shaped fragments of
sphene are frequently present in the rock, exhibiting the high relief
2i GEOLOGICAL SURVEY, CANADA
and interference colours characteristic of the mineral. Calcite is
also abundant as an interstitial and cavity ﬁlling constituent. Other
accessory minerals observed to occur are apatite and zircon as micro-
litic inclusions in the feldspar, garnet, magnetite, pyrite and hema-
tite.
Outside of an area near the north end of Morin lake, muscovite
is not a very prominent constituent of the foliated granitic rocks.
In the Morin Lake occurrence the mineral is chieﬂy developed along
cleavage lines traversing the gneiss. The mineral constituents of
the rock, with the exception of the change in the variety of mica
present, do not differ essentially from those found in the biotite
gneisses of the region.
In contradistinction to the biotite gneisses or granite, a variety
frequently occurs in which hornblende is the dominant coloured
constituent. This mineral occurs in large, strongly pleochroic, well
deﬁned fragments, idiomorphic to the feldspar and quartz surround-
ing it. The rock contains, like the biotite granite and gneiss, con-
siderable quantities of epidote, associated in this case with horn-
blende. The accessory minerals present are the same as in the other
varieties of gneiss, although the quantity of titanite and plagioclase
is rather more abundant.
In occasional localities the hornblende granite, or gneiss, is found
to pass into a syenite, or even to approach a diorite in composition,
by the loss of its quartz and alkali feldspar. This type of rock is
exempliﬁed by a pink, slightly gneissoid syenite, occurring on the
shore of Lao des Quinze to the south of its outlet. This contains the
usual minerals of a more basic type—hornblende, epidote and sphene
-—a little orthoclase, and an abundance of microcline and plagio-
clase, but no quartz.
Some other rocks of a basic character were observed associated
with the granite and gneiss, on the south arm of Lac des Quinze,
near its junction with the main body of the lake. The rock consists
of aggregates of hornblende, or of hornblende and biotite, enclosed
in feldspar, partially decomposed to saussurite. Occasionally dis‘
tinct crystals of hornblende can be observed in the section. Sphene,
epidote, calcite and magnetite are usually present, and sometimes a
few fragments of interstitial quartz occur. In some localities the
rock possesses a porphyritic appearance, due to the presence of the
dark hornblende aggregates surrounded by a light-coloured felds-
pathic matrix, while at other times, where the feldspar is less
EAST SIDE OF LAKE TIMISKAMING, QUE. 25
prominent, it becomes uniform and basic in appearance. The rela-
tionship of this rock to the granite in its southern border would
suggest that it had been enfoliated in the gneissic rocks. On the
west shore of the lake it is cut by granite dikes, while on the east
shore it has been broken up into a breccia, the matrix of the rock
consisting of granite.
Although both the Keewatin and the granitic rocks occur very
extensively in this area, contacts between the two are rarely exposed.
The granite and the quartz porphyrite were never observed adjoining
one another, although exposures of the two rocks were observed in
close proximity. The relationship of the granite to the Keewatin
diabase and schist is best shown along the northern border of the
Rousselot Lake greenstone area. The junction between the rocks was
seen at two points, one along the line between ranges IV and V, and
the other along that between ranges III and IV. Inthe former locality
the dividing line is exceedingly deﬁnite, with dikes of the granite
penetrating the adjoining greenstones; in the second the contact
is of a transitional type. The eifect of the dynamic action on‘ the
granite near the point of transition was well shown in a section
examined. The feldspars showed wandering extinction and were
much broken, the quartz had become granulated, and the biotite was
bent and frayed out at the margin. Calcite and pyrite were present
in abundance. '
Huronian.
The Huronian formation, as found in the district adjoining the
east side of Lake Timiskaming, is composed of the usual series of
fragmental rocks, following one another in regular and conformable
succession. The basal member of the formation is usually a con—
glomerate, containing pebbles and boulders of granite, diabase,
quartz-porphyrite, and other eruptiveswenclosed in a matrix of vary-
ing texture and composition, the latter depending, in part at least,
on the character of the adjacent underlying rock. The basal con-
glomerate, as a rule, passes upward into greywacké by the gradual
loss of its pebbles and boulders, the greywacké in its turn being- re-
placed by quartzite or arkose. This last mentioned rock is followed
in a few local areas by an upper coarse conglomerate. While the
above sequence is that found in the most typical sections, it is not
always so complete. Patches of arkose, or of greywacké, are some—
times found included in the conglomerate. Occasionally the grey-
26 GEOLOGICAL SURVEY, CANADA
wacké is entirely wanting, the conglomerate passing into quartzite;
or we may have arkose resting directly on granite, without the pre—
sence of the intervening conglomerate or greywacké. For mapping
purposes the conglomerate and greywacké have been separated from
the remaining upperpart of the series, the intimate and varying
association of these rocks making any further subdivision imprac-
ticable. On the whole these rocks have not been greatly disturbed,
usually occurring in gentle undulations, with 'a dip rarely exceeding
20°.
The relationship of the Huronian clastics to the various older
rocks of the district is such as to indicate that they were deposited
on a greatly decayed surface, such as may now be observed in some
of the non-glaciated regions Of the earth. Actual contacts between
the conglomerate and the Keewatin greenstones were never Observed,
although exposures of the two rocks are sometimes found within a
few feet of one another. The quartz-porphyrite and the con-
glomerate, however, were found adjoining one another in at least
two localities. '
On the point which occurs at the south end of Cameron lake, on
lot 30, range II, Laverlochere, a small area of conglomerate occurs
overlying the quartz-porphyrite. Pebbles and boulders of the latter
are enclosed in a base, which in places can scarcely be distinguished
from the included fragments, the whole of the conglomerate having
evidently been formed by the decomposition of the rock surface
beneath. A very similar association of the two rocks occurs on lot 5,
range IX, Guigues. Here, as on Cameron lake, the base of the con-
glomerate consists wholly of debris derived from the porphyrite;
but, as we get farther away from the Keewatin eruptive, fragments
of other rocks appear, the pebbles and boulders also become better
deﬁned and less angular, and the coarse, dark-green cementing
material becomes ﬁner grained. and more uniform.
The contacts between the Huronian and the older granites exhibit
this transitional relationship in a still more striking manner. A
very detailed description of one of these, occurring on the south
shore of Baie des Peres, has been given by Dr. Barlow, in which he
points out the various stages in the disintegration of the granite,
and the resultant formation of the overlying arkose. In the northern
part of range IX, Duhamel, a similar degradation of the granite
surface is shown in a section over 200 feet in thickness, consisting
of boulders and fragments of granite enclosed in an arkose matrix.
EAST SIDE OF LAKE TIMISKAMING, QUE. 27
In this locality the feldspar of the underlying rock is white in colour,
and has not undergone the sericitic decomposition to such an extent
as that on the lake shore, in consequence of which there is so little
contrast between the two rocks that the line of junction cannot be
ﬁxed within a wide latitude. The slight mechanical action to which
the disintegrated granitic material has been subjected also makes it
exceedingly diﬁicult to distinguish the matrix from the enclosed
fragmental masses.
Junctions between granite and conglomerate of a transitional
type were observed in two other localities in the region, namely, on
the Shore of Lake Timiskaming opposite Drunken island, and at the
east end of lot 30, range I, Laverlochere. In the ﬁrst lrcality the
granite surface is covered by a thin layer of arkose, followed imme-
diately by conglomerate, containing the usual pebbles of granite,
diabase and other eruptives, enclosed in a reddish matrix. In the
second locality the rocks are associated in the usual transitional way,
the base of the conglomerate being composed of closely compacted
pebbles and boulders of the underlying granite porphyry. This fact,
in view of the very limited extent of this porphyrite variation in the
granite, would indicate the extremely local origin of the conglo-
merate.
A contact between the Huronian conglomerate and the granite
was observed, however, on the shore of Lake Timiskaming, on lot 18,
range I, Fabre, which is of a very diﬁerent type to those so far
described. The junction between the two rocks is not transitional,
but very deﬁnite. In this case the conglomerate has evidently not
been derived from the granite by its disintegration in situ, but
obtained its material, to a large extent at least, from foreign sources.
The few feet of the contact exposed do not permit of an extended
examination; but the way in which the conglomerate ﬁlls in the
hollows in the granite surface, the close resemblance between the
border of the granite and an eroded surface, and the absence of any
evidence of metamorphism in the conglomerate, seems to prove that
the granite is unconformably overlain by the Huronian. The junc-
tion at this point is no doubt a continuation of that occurring on
the west side of the lake, some distance farther south, which Dr.
Barlow describes as follows: ‘ The line of contact in the immediate
vicinity of the lake runs in a general direction S. 75° W., but this
line is not perfectly straight, as the granite has a somewhat sinuous
edge, which is followed very faithfully by similar irregularities in
28 GEOLOGICAL SURVEY, CANADA
the schistose structure of the breccia-conglomerate. It is quite
evident from an inspection of the coarser fragments that they have
not been derived from the disintegration of the gneissic rocks with
which these clastics were in contact, for the minerals composing
them are much coarser in their method of crystallization, and of a
deeper red colour, resembling closely in these particulars the granite
exposed on both shores of the lake to the north of Old Fort
Narrows.’1
CONGLOMERATE AND GREVWACKE.
The Huronian conglomerate and greywacké, while not usually
occurring in extensive areas, are widely distributed in the region,
either in small isolated outcrops, or as narrow bands at the base of
quartzite ridges. The latter type of occurrence is best exempliﬁed
in the cross sections of Huronian rocks to be found on the shores of
Lake Timiskaming, as on the south Side of Lavallée bay or of Joanne
bay. The largest exposed area of these racks is that occupying
the southwestern part of Laverlochere township, extending from
Otter lake to range I, and from Rousselot lake to range VII
of Fabre township. There are some portions of this area which
might be more properly mapped as arkose; but their intimate asso-
ciation with the conglomerate or greywacké, and their limited extent,
did not permit of their separation. From the number of outcrops
of conglomerate and greywacké occurring along the watercourses in
the clay-covered areas, it is probable that a large proportion of the
clay ﬂats are underlain by Huronian, and that the exposed portions
form only a small part of the area of these rocks actually present in
the region.
The Huronian basal conglomerate, sometimes referred to as slate
conglomerate, chlorite slate conglomerate, or breccia-conglomerate,
is a massive rock, as found in the region in question, exceedingly
variable both as regards its included fragments and the ﬁner-grained
material enclosing them. On the weathered surface the rock is
usually white, grey or greenish-grey in colour, the greenish Shade
being particularly noticeable where the rock is not freely exposed to
the atmosphere.
All the pre-Huronian rocks of the region are represented among
the pebbles and boulders of the conglomerate; but, as indicated by

1 Annual Report Geol. Surv. Can., Vol. X, p. 189 I.
\‘-
EAST SIDE or LAKE TIMISKAMING, QUE. 29
the majority of the contacts described above, their relative abund-
ance is largely controlled by the variety of rock lying immediately
beneath. Granite is by far the most frequent of the included frag-
ments; but diabase, quartz-porphyrite, green schist, jasper and
quartz are also present. Although these are sometimes angular or
subangular in outline, especially so in the transitional contact zones,
on the whole they are moderately well rounded, exhibiting all the
characteristics of water-worn littoral or possibly ﬂuvitile debris. The
included fragments are usually numerous, and are frequently so
closely compacted as to leave little room for interstitial material.
They vary in size from pebbles to boulders two or three feet in
diameter.
The detrital material forming the matrix of the rock, as the
name slate conglomerate would imply, most frequently has a greenish
slate-like appearance, which, when examined microscopically, is
found to consist of fragments of quartz and feldspar, included in a
groundmass, consisting largely of chlorite, sericite, and epidote.
There are, however, a number of localities in which the enclosing
material is comparable to an arkose or feldspathic quartzite in com—
position, consisting almost wholly of coarse, angular fragments of
feldspar and quartz.
As the basal conglomerate is followed upward, the pebbles and
boulders generally disappear, the rock becoming greywacké, which is
identical in composition with the ﬁner—grained, slaty matrix of the
conglomerate. Under the microscope the rock consists of grains and
irregular fragments of quartz, orthoclase, microcline, and plagioclase,
embedded in a groundmass, chieﬂy composed of chlorite and sericite,
though epidote, leucoxene, hematite, magnetite, ilmenite and tour-
maline were also observed in some sections. Sir Wm. Logan in
' describing his chlorite slates, the equivalent of what we have termed
greywacké, states ‘ that sometimes the rock has a semblance of por-
phyry, appearing to contain opaque white crystals of feldspar; but
these are more probably small angular fragments of the mineral.’1
This property of the rock can be observed on Drunken island and on
the greywacké ridge which forms the southern boundary of the valley
of the Little river. It was in the former locality, no doubt, that
Sir Wm. Logan made his observations. A similar pseudo-porphy-
ritic rock occurs at Wright mine, in association with the ore

1 Report of Progress. Geol. Surv. Can., 1845-6, p. 67.
30 GEOLOGICAL SURVEY, CANADA
Q
deposit, but in this case grains of quartz are also present. Al-
though the greywacké as a rule is structureless, massive rock, it
sometimes occurs, in local areas more especially, either in associa-
tion with conglomerate or near its contact with the overlying
quartzite, well stratiﬁed and delicately banded in various shades of
green and red.
QUARTZITE, ARKOSE, AND CONGLOMERATE.
The quartzite, arkose, and conglomerate, the topmost members of
the Huronian series, while by far the most extensive of the Huronian
rocks in the region, are practically conﬁned to the townships adjoin-
ing the east side of Lake Timiskaming. With the exception of the
small bands of conglomerate, greywacké or granite occurring at the
base of the hills or ridges, all of the rock exposed in the southwestern
part of Cruigues, the whole of Duhamel, and the northern part of
Fabre, consists of arkose or quartzite.
The association of these rocks with the conglomerate and grey-
wacké is worthy of note, because of the unconformable relationship
between the two parts of the series described by Prof. Miller as
occurring on lot 4, in concession XII of Lorrain, on the
basis of which he has classed the arkose and quartzite as middle
Huronian. The gradual transition of the conglomerate and grey-
wacké upward into quartzite can be observed on the south shore of
Lavallée bay, on a point to the south of Joanne bay, on the shore
of the bay to the north of Wright mine, and on the slope of the
ridge which parallels the Quinze roadl across ranges IV and V,
Duhamel. In all of these localities the underlying rock passes into
quartzite by the gradual introduction of the coarser quartzose grains,
without the slightest evidence of a structural break.
Where this upper portion of the Huronian occurs in direct con-
tact with pre-Huronian granite, the rock is a typical arkose; but
in those portions more remote from the granite, upon which
katamorphic agencies have been at work, it becomes a quartzite.
Between these two extremes all gradations exist, the predominat-
ing type of rock being a feldspathic quartzite. In ranges V and
VII of the township of Fabre, some areas of quartzite
occur which are overlain by conglomerate not unlike some of the
coarser phases of the basal member of the series. There are also
some localities, very numerous in the vicinity of Ville Marie, where
.wm x 5.523.: BEA .EETH ragga “amnesia @535 5 9:2 ﬂoEoewZIﬁ 52H .wm v. EEG .533 .Es: @3555... a5§§§ahlé .m;


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EAST SIDE OF LAKE TIMISKAMING, QUE. 31
the quartzite contains bands of well rounded pebbles of jasper and
quartz, forming-a rock somewhat similar to the jasper conglomerate
of the north shore of Lake Huron, but distinguished from it by its
granular and less massive groundmass. These rocks usually show
some trace of stratiﬁcation, and occasionally, near their contact with
the underlying greywacké, are very perfectly bedded. Examined
microscopically, sections of the rock are found to consist of a mosaic
of rather angular grains of quartz, plagioclase, orthoclase and \micro-
cline, the feldspars being in various stages of alteration to sericite
and epidote. The interstitial material is usually limited in quantity,
and apparently derived to a large extent from feldspathic decomposi-
tion, though small quantities of minerals from other sources, such
as chlorite, magnetite, hematite and pyrite occur.
ORIGIN OF THE HURONIAN ROCKS.
From an examination of the Huronian clastics, it would seem
quite probable that the underlying basement had been the source of
all the materials of which they are composed. If such be the case,
we must then consider the whole formation as a series of sediments,
deposited upon an uneven and greatly decayed surface, the unusual
thickness and extent of the conglomerate being due to the immense
amount of fragmental material which had accumulated, and to the
disintegrated condition of the rock surface. The transition which
occurs from granite through arkose to quartzite, and the frequent
and undoubted bedding planes which occur in the quartzite, seems
to prove that the upper portion of the formation originated in this
way; but the mode of origin of the conglomerate and greywacké
is not so evident, as might be indicated by the differing opinions
expressed on the subject by various authorities. These rocks have
been described as volcanic breccias, as sediments, or combinations of
the two, and quite recently Professor Coleman has presented argu-
ments in favour of their glacial origin.1 As regards the conglomerate
and greywacké, as they occur on- the east side of Lake Timiskaming,
there seems to be little basis for the volcanic hypothesis. The most
typical breccia conglomerate occurs at those points where the en-
closed fragments can be directly connected with the adjacent under-
lying rocks. Nowhere were included fragments observed which might
be described as bombs, scoriae or other materials resulting from vol-

a
lJournal of Geo, V01. XVI, 1908, p. 149.
32 GEOLOGICAL SURVEY, CANADA
canic activities of an explosive type, nor do any effusive rocks occur
in the district such as would probably accompany such an extended
eruption. There does not appear to be any conclusive evidence, in
the area in question, whether the conglomerate and greywacké on the
whole represent water-laid sediments or a tillite, deposited during a
glacial epoch, as advocated by Professor Coleman. The contacts
between the Huronian and the Older eruptives, however, with but
one exception, show that the basal portion of the conglomerate
originated by the degradation in situ of the underlying rock surface,
and hence this part at least has not been glacially deposited. As to
the remainder of the conglomerate and the greywacké, there is no
deﬁnite evidence of extended sedimentation, although local areas of
well stratiﬁed greywacké, often intimately associated with the con-
glomerate, are of frequent occurrence. It is nevertheless worthy of
note that the remarkably uniform gradation from conglomerate up-
wardinto greywacké, not only in this area but elsewhere throughout
the Huronian of the Timiskaming district, is characteristic of sedi~
mentation following a widespread submergence rather than glacial
deposition, interrupted by several interglacial periods.
DIABASE AND GABBRO.
If the few outcrops of diabase occurring in the township of
Fabre, which probably form part of an intruded sheet or sill, be
excepted, the post-Huronian diabase or gabbro is represented on the
east side of Lake Timiskaming by merely a few dikes, the largest
of which does not exceed a third of a mile in width. These occur
most frequently cutting the granite and gneiss, their contacts with
the adjoining rock being always very sharply deﬁned. They are
usually coarse in the centre, becoming ﬁne-grained and trap-like on
the border.
One of the largest of these dikes was observed crossing the north
end of Blueberry island in Lake Kipawa. Macroscopically this is a
porphyritic rock consisting of large phenocrysts of very dark labra—
dorite enclosed in a dark-grey Ophitic groundmass. On the weathered
surface, the ﬁne-grained matrix enclosing the labradorite crystals
becomes a rusty-brown colour, while the phenocrysts show up white
or pink. Examined under the microscope, the rock was found to
consist essentially of olivine, plagioclase and augite, and hence may
be described as a porphyritic, olivine diabase. The plagioclase,
though very fresh in appearance, is clouded with a ﬁne brown dust,
EAST SIDE oE ,LAKE TIMISKAMING, QUE. 33
the composition of which was not determined. The ophitic structure
is well shown in the thin section, the feldspar occurring in lath-like
idiomorphic crystals. From determinations of the extinction angle
in sections at right angles to the albite twinning plane, the plagio-
clase was found to be labradorite. This mineral exhibits not only
the usual albite twinning, but also the pericline, and occasionally
the carlsbad law. The augite is abundant, occurring in well deﬁned
light-brown, slightly pleochroic fragments, showing very distinctly
the cleavage characteristic of the mineral. The olivine occurs in
round or oval fragments, which in section appear almost colourless.
The mineral is always fresh, but wherever it adjoins the labradorite
it is bordered by a double zone of reaction products, the
outer of which consists of light-green hornblende, and the inner
of colourless pyroxene. Both of these zones, where examined under
crossed nicols, show a distinct radial arrangement from the olivine
centre outward. The outer hornblende zone is usually ﬁbrous, but
occasionally shows the prismatic cleavage of the amphibole group,
while the pyroxene, on the other hand, possesses the rectangular
cleavage which characterizes that mineral. This phenomena is pre-
cisely similar to the reaction series described by Adams,1 Williams2
and a number of other authorities. Fragments of ilmenite are very
numerous throughout the section, usually associated with the olivine,
and always enclosed in a border of deep—brown, strongly pleochroic
mica, resulting apparently from the interaction of the olivine, plagi-
oclase and ilmenite. A few hexagonal and rod-like crystals of
apatite also occur scattered throughout the feldspars. The order of
crystallization is very clearly indicated in sections of this rock. The
olivine and ilmenite were the ﬁrst minerals to crystallize, the
ilmenite being generally included in the olivine, which always
presents a round or elliptical form. The labradorite crystals were
then formed, followed by augite, which ﬁlled in the remaining inter-
stitial portions of the rock. A reaction seems to have gone on
around the border of the olivine during the crystallization of the
feldspar, forming the double zone of pyroxene and hornblende, when
olivine alone was present, but when in association with ilmenite,
resulting in a more basic ferro-magnesian mineral, probably lepi-
domelane. The augite, on the other hand, whenever it occurs
adjoining either the plagioclase or the olivine, presents a very

1 Am. Nat., 1885.
2Am. Jour. of $0., 1886.
6487—3
34 GEOLOGICAL SURVEY, CANADA
deﬁnite boundary, conforming to the outline of these minerals, being
concave when in contact with the olivine, and straight in the case of
the plagioclase.
- All the diabase dikes observed in the area, with the exception of
that of olivine diabase just described, have a general northerly and
southerly direction. This fact, together with the similarity in the
rock itself, would indicate a common origin for the whole series.
They are composed of a grey or greenish-grey rock, with a more or less
distinctly diabasic structure. Microscopically the rock is found to
contain an abundance of the usual idiomorphic plagioclase, showing
twinning according to the albite, or albite and pericline laws com-
bined. The mineral is usually fresh, but occasionally the incipient
stages of saussuritic alteration are to be observed. Granophyric in-
tergrowths of orthoclase and quartz sometimes occur, ﬁlling in the
interspaces between the other minerals. The augite is sometimes
twinned, and is usually characterized by the basal and prismatic
cleavage of the proxene group. Its boundaries are well deﬁned and
allotriomorphic, it being one of the last minerals generated. Biotite,
pyrite and magnetite were also found in many of the sections, while
calcite and epidote were occasionally observed.
These dikes occur widely distributed, though usually not exposed
for any great distance. One of the longest observed occurs about
one mile east of the outlet of Lac des Quinze, extending in a north
and south direction across the lake, and then fringing the east shore
of the lake for nearly two miles. This dike is paralleled by a
number'of others crossing the islands in the head rapids of Riviere
des Quinze. Another of these dikes that might be mentioned is that
extending in a northeasterly direction from the north end of Otter
lake, and reaching to lot 13, range XI, Laverlochére.
The diabase, which occurs in the township of Fabre, is so poorly
exposed that it is difﬁcult to determine its actual extent, or to gather
any evidence as to its relationship to the other rocks in its Vicinity.
Its examination is further obscured by the great amount of chemical
alteration and mechanical deformation which has taken place in the
rock, so that even the freshest specimens obtainable are for the most
part a mass of decomposition products.
While it is quite probable that all the Fabre diabase forms part
of one intrusive sheet, it occurs in two separate 'areas, one on the
lake shore in the vicinity of Lavallée bay, and the other about two
miles farther inland. The Lavallée Bay area comprises the rocky
\
vs riders


Fig. L—Diabase neg; Fabre Wharf x 28.
P LATE V.
Fig. 2.—Intergrowth of Feldspirs in


Diabase, Fabre township {28.
EAST SIDE OF LAKE TIMISKAMING, QUE. 35
knob which occurs at Fabre wharf, and the rugged outcrops which
form Quinn point a short distance farther north. The exposures of
this rock in the interior part of the township form a triangular area,
the western border of which extends from the middle of lot 20, range
III, Fabre, northward to the western extremity of lot 34, range IV.
Its northern limit extends eastward from the last-mentioned point
across the south end of range V north, meeting the granite just
outside the surveyed ranges. Its southeastern boundary is de-
limited by its junction with the granite, which maintains a general
southwesterly direction, crossing the line between ranges V south,
and VI south, on lot 11, and that between VI and VII south, on lot
3, range IV.
The Fabre diabase is a greenish-grey rock, presenting in some
localities the appearance of a ﬁne-grained diabase, but in others
resembling a coarse diorite. In the coarser dioritic varieties an
abundance of fragments of ﬁbrous hornblende derived from the
alteration of the augite is very characteristic of the rusty weathered
surface. The rock is so greatly decomposed that its microscopic
examination is very unsatisfactory. Plagioclase is always abundant,
but is frequently completely altered, the idiomorphic outline of the
mineral, however, being usually apparent. Peculiar intergrowths of
orthoclase and plagioclase are sometimes present in the rock,
as ' well as micropegmatitic intergrowths of quartz and feldspar,
Throughout the greater part of the sections examined the alteration
of the augite to hornblende was nearly complete, the uralitic product
presenting a ﬁbrous or a minutely columnar structure. Calcite,
ilmenite and pyrite are the other constituents of the rock, the iron
ores being usually abundant. The ilmenite is often altered to
leucoxene in lamellar parallel rhombohedral lines, resulting in a
gridiron structure.
As far as can be learned from its ﬁeld relationships, the Fabre
diabase is post-Huronian in age, although the evidence is not as
conclusive as might be desired. The outcrops of conglomerate and
greywacké which occur in its vicinity have been greatly tilted and
metamorphosed, the pebbles of the conglomerate being elongated and
a distinct foliation imparted to the greywacké, parallel to the dia-
base margin. On its eastern limit the rock is in contact with the
granite border of the gneissic rocks, but the junction where exposed
is of such a transitional character that no evidence has been obtained
as to whether the two rocks are contemporaneous in age or one intru-
6487 —3:§
36 GEOLOGICAL SURVEY, CANADA
sive through the other. A section of the intermediate type of rock
was found to contain a considerable amount of rather fresh quartz,
but otherwise showed no evidence of dynamic action.
Silurian.
CLINTON AND NIAGARA.
The Silurian syncline which occupies the north end of the TimiS-
kaming depression, by reason of its isolated position and abundant
fossil fauna, has attracted the attention of geologists for a number
of years. It was described by Sir Wm. Logan, ﬁrst in 1845, then
more fully in the Geology of Canada in 1863. The names of thirteen
species collected from the outlier and identiﬁed by Mr. E. Billings
are mentioned in the latter publication. Additional collections of
fossils made by Dr. Bell in 1887, and by Dr. Barlow in 1892-4, were
identiﬁed by Dr. Ami and Mr. L. M. Lambe. From the determina-
tion of these fossils, Dr. Ami placed the rock in the Clinton or
Niagara, the species being for the most part forms referable to the
Niagara, although a number occur which belong rto rocks assigned to
the Clinton formation. He also points out the similarity in fossil
fauna of this area with the Silurian of Lake Huron rather than with
that of the Hudson Bay and Winnipeg basins.
The rock comprising this Silurian outlier is a limestone, usually
ﬁne-grained but becoming coarse and fragmental near its junction
with the adjacent underlying rock. It is found on the east side of
Lake Timiskaming merely as small, basal remnants fringing the
lake shore. Thus, on the Shore opposite Bryson island, to the north
of Joanne bay, and in the bay to the north of Wright mine, small
patches of an arenaceous well-bedded limestone occur, dipping from
5° to 10° to the southwest. The Shore of the lake between Piché point
and Chief island is bordered by a fringe of conglomerate and sand-
stone, the sandstone forming a sort of terrace along the high-water
margin of the lake. Between this and the water’s edge the rock
consists of fragments and hummocks of the quartzite ﬂoor enclosed
in a calcareous matrix, in which some fragmental fossil remains are
present. At the east end of lot 19, range II, Guigues, a small out-
crop of calcareous, non-fossiliferous sandstone is exposed, dipping 5°
in a southwesterly direction. The occurrence of this outlier so far
inland and nearly 150 feet above the level of Lake Timiskaming,
would indicate that the Silurian had been originally very much more
extensive in the area than at present.
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6457
EAST SIDE OF LAKE TIMISKAMING, QUE. 37
Pleistocene.
The pleistocene deposits of the area east of lake Timiskaming
are very closely related to the work of the glacial ice sheet. The
material dropped by the glacier is found, to a large extent, scattered
irregularly over the surface, without assuming many of the forms
characteristic of glacial deposition, although a few ridges of gravel
and sand occur, which probably represent terminal moraines, two
of the best examples of these being the ridges east of the north end
of St. Amant lake, and that which crosses Lake Timiskaming at Old
Fort Narrows. In the eastern rocky portions of the area mapped,
the pleistocene consists wholly of this glacial debris, but in the
vicinity of Lake Timiskaming the depressions of the surface have
been ﬁlled in with post-glacial clay. These clays are well stratiﬁed,
and in the vicinity of the lower part of the basin of the Otter river
have a distinct terrace form, probably representing stages in the
retreat of the post-glacial lake.
Economic Geology.
Gold—Quartz veins are very numerous throughout all the rock
formations found in the area, but occur most extensively traversing
the granites, and interfoliated with the gneisses. These usually
contain small quantities of disseminated pyrite and chalcopyrite,
and occasionally galena, the latter being most abundant in the
Huronian. These veins are not, as a rule, auriferous, or if gold is
present the percentage is not high enough, or the quantity of ore
sufﬁciently large, for proﬁtable operation.
Siloer.—The proximity of the east side of Lake Timiskaming to
the silver-bearing district of Ontario has directed the attention of a
large number of prospectors to this area during recent years, but so
far the results have been largely negative. Since the post-Huronian
diabase, with which the silver-cobalt ores of the Timiskaming area
are associated, has its largest extent in the township of Fabre, these
minerals are more likely to occur in that district. The diabase
occurring in Fabre township, however, is so poorly exposed that
prospecting is rendered very difﬁcult, and although a number of
minerals have been found in small quantities in the rocks, no de—
posits of economic importance have as yet been discovered.
38 GEOLOGICAL SURVEY, CANADA
An occurrence on lot 5, range V north, of Fabre, which is being
developed by the Pontiac Mining and Milling Company, is worthy of
attention, because of its similarity to the silver-bearing series of
James township and elsewhere in that vicinity. On the surface the
deposit consists largely of specularite, with sulphides of copper and
iron, but these are replaced immediately beneath by red feldspar and
calcite, carrying small quantities of galena, pyrite and chalcopyrite.
Examined microscopically, the orthoclase was found to be very fresh,
and frequently twinned according to the Carlsbad law, while the cal—
cite was observed to ﬁll in the cavities and interstitial portions of the
sections as if of secondary origin. Some fragments of epidote also
occur, as well as grains of the sulphides mentioned above. The
proportion of feldspar and calcite in the vein is exceedingly vari-
able, some parts consisting almost wholly of feldspar, while in others
the calcite predominates. Sometimes pure calcite occurs up to 6”
in width, ﬁlling what are apparently secondary fractures in
the vein-matter. .There does not appear to have been any marked
ore-concentration in the formation of these veins; the calcite is
entirely barren and the quantity of sulphides unimportant. An
assay of a specimsn of the average type of vein-matter, made by Mr.
M. F. Connor of this Department, yielded 3-12 ounces of silver per
ton of 2,000 pounds. From this result it seems probable that the
silver values in the vein arise solely from the galena present, so that
those portions in which galena is more concentrated would give a
much higher silver content than the above. The shaft on the
property has been sunk to a depth of about 50 feet, the vein having
a maximum width in that distance of 3 feet.
The most important and interesting ore deposit of the east side
of Lake Timiskaming is the property known as Wright mine, which
comprises the western parts of lots 61, 62 and 63, range I, Duhamel
township, shown on the maps as Blocks A and B. The ore body,
which is exposed on the water-worn rock surface of the lake shore,
was observed by the early French explorers, since the location is
marked Ansé a la mine on a map of the lakes of Canada published
in 1744, a print of which appears in Professor Miller’s report of
1905.1
The rock in the neighbourhood of the mine is the Huronian con-
glomerate, but adjacent to and included in the deposit it assumes


1Report of Bureau of Mines, Pt. II, 1905, p. 43.
EAST SIDE or LAKE TIMISKAMING, QUE. 39
a porphyritic appearance, very similar to the greywacké occurring
on Drunken island. Examined in section this is found to consist of
fragments of quartz and feldspar enclosed in a granular groundmass
of the same minerals. An abundance of chlorite, as well as some
calcite and ilmenite, occur throughout the ﬁner-grained material.
The quartz fragments are generally corroded on the margin, and the
feldspars clouded with decomposition products. The ore deposit
occurs in a brecciated zone in this porphyritic phase of the con-
glomerate, fragments of the rock being completely enclosed in calcite
and galena, which also contains small quantities of iron and copper
pyrites.
Operations on this deposit were ﬁrst begun in 1886, by Mr. C. V.
Wright, of Ottawa, but no extensive work was carried on until 1890,
when the property was acquired by the Mattawa Mining and Smelt-
ing Company. A very complete plant was installed and mining
actively prosecuted until March, 1891, when work was suspended.
From 1896 to 1902 the mine was operated in a small way, ﬁrst by
the Petroleum Oil Trust and later by the British Canadian Lead
Company, both of these corporations representing English capital.
Quite recently the property has again changed hands, the present
owners being the members of the La Rose Mining Company, of
Cobalt. Active mining, however, has not been resumed. At the
time of the suspension of work in 1902, a depth of 250 feet had been
reached in the main shaft, while short drifts had been made at the
65, 100, 200, and 250 ft. levels.
A number of assays of the ore from this mine have been made,
both in this department and by private assayers. The galena entirely
free from gangue is found to yield from 13 to 26 ounces of silver
to the ton, with about 18 ounces as a mean value. It is also found
to have a lead content of about 52 per cent, and usually yields traces
of gold. The values obtained in operation were greatly diminished, -
however, by the large amount of rock which had to be mined and the
consequent crushing and concentrating which this involved. During
the earlier part of its history the lack of transportation facilities was
also a difﬁculty.
The origin of this irregular deposit is very obscure. The vein-
matter has no doubt been deposited by replacement along a
zone of fracture or brecciation in the Huronian, though the imme-
diate cause of the brecciation of the conglomerate is not apparent.
The occurrence of the ore in association with the porphyritic varia-
40 GEOLOGICAL SURVEY, CANADA
tion in the conglomerate is probably a mere coincidence, similar
porphyritic rocks occurring quite frequently in the Huronian, as on
Drunken island, and in the greywacké ridge which forms the
southern boundary of the valley of the Little river.
Copper.——Small vein-like deposits of iron pyrites occasionally
occur throughout the Keewatin greenstones. These usually contain
a very small percentage of copper, due no doubt to chalcopyrite
disseminated through the iron sulphide. The Jessie Fraser Copper
Mining Company has been engaged during the last two years in
developing one of these sulphide deposits, which occurs on lot 8,
range VII north, Fabre township. In this occurrence the schist ad-
joining the deposit sometimes shows a thin ﬁlm of native copper
along the lines of parting. Quartz veins containing chalcopyrite
and pyrite are very abundant in the area. Thus, on lot 7, range V
north, of Fabre, these minerals occur associated with an irregular
quartz vein traversing the Keewatin quartz-porphyrite. The sul-
phides have been impregnated through the rock to a width of four
or ﬁve feet at some points, but the quantity of chalcopyrite so far
disclosed by development work is unimportant.
Iron—The iron ranges which were observed in the district have
already been described under the rocks of the Keewatin formation.
In neither of the two localities mentioned, Lac Clair and Kakake
lake, is the ore body high enough in iron content, or of sufﬁcient
extent to be Of economic value.
Asbestos.-—Fibrous serpentine occurs in small veinlets traversing
the Keewatin serpentine rock of range VII, Duhamel, but the
quantity of the material is not extensive, nor its quality of very high
grade.
Limestone—The occurrence of the Silurian limestone at the
north end of Lake Timiskaming is of great economic importance,
both on account of its accessibility, and the limited extent of the
rock in the region from Lake Timiskaming northward. It can not
only be used for the manufacture of lime, but also makes a very
excellent building stone. Professor Miller gives the following
analysis of the rock as found at Farr’s quarry, Haileybury:-——
EAST SIDE OF LAKE TIMISKAMING, QUE. 41

Percent.
29-50
Magnesia.......................... 21-59
Ferric oxide and alumina.. .. .. .. .. .. .. 0-66
Insolubleresidue.................... 1-60
Carbondioxide............ .. .. 46-84
Sulphurtrioxide.................... 0-70
Total........................ 100-89
Clay.—The stratiﬁed clays which occur so extensively on the east
side of Lake Timiskaming are well adapted for the manufacture of
brick and earthenware, but are more important from an agricultural
standpoint. A large part of the clay flats in the district has been
cleared, and now supports a numerous and prosperous farming com-
munity. The central distributing point for the settlement is the
village of Ville Marie, situated on the lake shore at the foot of the
very picturesque inlet known as Baie des Peres.
INDEX.
A
Agricultural land .. .. .. .. .
Page.
Ami, Dr., report on fossils referred to.. .. .. .. .. .. .. .. .. .. .. ..
C!
Timiskaming fossils identiﬁed by. .
Al‘ea examined deﬁned.. .. . . .
Arkose.. .. .. ‘
Asbestos. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..
Baby area .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..
P-aie des Peres“ .. .. .
Hallow, Dr.
granite.. .. .. .. .
(f
{f
(f
Bell, Dr. R., fossils collected by.. .. .. .. .
Billings, E., Silurian fossils of Timiskaming identiﬁed by.. ..
Nipissing and Timiskaming map sheets .. .. ..
Timiskaming fossils collected by.. .. .. .. .. ..
work under direction of.. .. .. .. .. .. .. .. ..
A. E., description of contact between Huronian and
. .26,
BIitish Canadian Lead 00., operators of Wright mine“ .. .. .. ..
C
Clays, stratiﬁed.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .
Clinton formation.. .. .. .. .. .. .. .. .. .. .. .. .
Coleman, Prof., re glacial origin of Huronian rocks... .. ..
Conglomerate.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .
“ and greywacke.. .. .. .. .
“ included in Huronian.. . . .
(f (6'
Keewatin.. .. .. .. .. .. .. .. .
Connor, M. F., assay by.. .. .. .. .. .. .. .. .. .. .. .. .. .
Copper“ .. .. ..
Diabase and gabbro.. .. .. .. ..
Duhamel area.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..
0' an I. 'I ll 00 no on 00 II o. 00 on
Fabre area.. .. ..
Farr’s limestone quarry.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..
Q. I. O. I. O. .I c0 .0 0- on 0| l
. .13,
. .13,
41
36
30
40
13
41
27
36
36
36
39
41
36
31
30
28
25
18
38
40
14
37
14
40
36
44¢ INDEX'
G
Gabbro.. .. .. .. .. .. .. .. .. .. .. ..
Galena.. .. .
Galt-St. Amant-Morin chain of lakes. . . .
Geology of the district .. .
Glaciation.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..
Cold .. .. .. .. ..
Granite and gneiss.. .. .. .. .. .. .. .. ..
Greenstone, peculiar variation of.. .. ..
Greenstones.. .. .. .. .. .. .. .. .. .. .. .. ..
“ and schists, transition between ..
If
Greywacke . . .
H
Huronian conglomerate at Wright mine.. .. .. ..
“ formation.. .. .. .. .. .. .. .. .. ..
" “ different from that at Cobalt..
rocks, origin of.. .. .. .. .. .
11.0.11 00 I. 0. I. .0 0' D. II a. I. a. In 0' I. .0 0. 0|
II .- O. .0 II .0 O. O. I. 00 I. 00 00 I. O. QC .0 no .0 I.
J aspilite. . . .
Jessie Fraser Copper Mining Co... .. .. .. .. .. .. .. .. .. .. ..
I K
Kakake lake, iron ore at.. .. .. .. .. .. .. .. .. .
Keewatin.. .
Lao Clair area.. .. .. .. .. .
((
iron ore at.. .. .. ..
Lambe, L. M., Timiskaming fossils identiﬁed by.. .. .. .. .
La Rose Mining Co., operators of Wright mine.. .. .. .. .. .. .. .. ..
Laurentian.. .. .. .. .. .. .. .. .. .. .
Lavallee creek.. .. .. .. .. .. .. .. .. ..
Limestone.. .. .. .
Little river.. .. ..
Logan, Sir Wm., description of chlorite slates. .. .. .. .. .. .. .. ..
(6'
Ottawa river examined by.. ..
(6'
U l I Q I a I 0 I n O I l I O O O I I Q a 0 O
. ..13, 14, 16, 18, 19, 21, 25
Silurian of Timiskaming depression described by... 36
Lorrain granite.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..
Page.
.. .. .. 32
..37, 38, 39
9
.. .. 1'0
..13, 37
..37, 39
20
.. .. .. .. .. 15
. ..13, 14:, 15, 17
16
40
30
.. .. .. .. .. 38
. ..21, 25, 28, 30
11
31
17
a e 35,
.. .. 17
..14,40
40
. ..13, 14, 17, 18
40
36
39
20
40
29
KI
21
INDEX 45
M Page.
McOuat, W'alter, geological examination by.. .. .. .. .. .. .. .. .. .. 8
“ greenstone described by.. .. .. .. .. .. .. .. .. .. .. 15
jaspilite observed by .. .. .. .. .. .. .. .. .. .. .. .. 17
Maple rapids.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 14
Mattawa Mining and Smelting Co... .. .. .. .. .. .. .. .. .. .. .. .. 39
Miller, Prof., analysis of limestone rock.. .. .. .. .. .. .. .. .. .. .. 40
(f
“ designation of Lorrain granite.. .. .. .. .. .. .. .. .. 21
“ parallellism of watercourses..- .. .. .. .. .. .. .. .. .. 10
“ quartzite, arkose and conglomerate.. .. .. .. .. .. .. 30
‘4'
report on cobalt ores referred t0'.. .. .. .. .. .. .. .. 8
Mitchell mine.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..14, 19
Niagara formation.. .. .. .. .. .. .. .. .. .. .. .. .. .. . .. .. .. .. 36
O
Obalski,Mr., report referred to.. .. .. .. .. .. .. .. .. .. .. .. .. .. 8
Otter river.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 9
p s
Petroleum Oil Trust, operators of WVright mine.. .. .. .. .. .. .. .. 39
Physical features of area east of Lake Timiskaming.. .. .. .. .. .. .. 8
Pleistocene.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 37
Pontiac Mining and Milling Co... .. .. .. .. .. .. .. .. .. .. .. .. .. 38
Porphyrite.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 14
Pyrites, copper .. .. .. .. .. .. .. .. .. .. s. .. .. .. .. .. .. .. .. .. 39
“ iron.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..17, 39, 40
Q
Quartz porphyrite. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 18
Quartzite.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 30
“ included in Keewatin greenstones.. .. .. .. .. .. .. .. .. .. 18
R
Rousselot Lake area... .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..13,14
Serpentine rocks.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ..15, 1640
Silurian.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 36
Silver.. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 37
Surveys, method of making. .. .. .. .. .. .. .. .. .. .. .. .. .. .. 7
T
Timiskaming lake, character of shore 1ine.. .. .. .. .. .. .. .. .. .. 36
46 INDEx
V
Vermillion district of Minnesota, comparison with.
Ville Marie.. .. .. .. .. .. .. .. .. .. .. .. .. ..
W
Wright mine. . . . . .
Y
Young creek. .. .. .. .. .. .. .. .. .. .
Page.
17 i
4.1
.. .. .. .. .. .. .. .. .. .. .. .. .. . ..29, 38
Wright, C. V., operation on \Vright mine commenced by.. .. .. .
39
Hon. W. TEMPLEMAN,
CANADA
DEPARTMENT OF MINES
GBOLO GICAL SURVEY BRANCH.
MINISTER ;
R. W. Bnocx,
A. P. Low,
DIRECTOR.
DEPUTY Mxmersn;

SELECTED LIST OF REPORTS AND MAPS
(SINCE 1885)
OF SPECIAL ECONOMIC INTEREST
PUBLISHED BY
THE GEOLOGICAL SURVEY.
Reports of the Mines Section:—
No. 245. Report'of Mines
272 a
300
301
334
335
360
572
602
625
Mineral Production of Canada:—
{I
(1'
manna-S
:“ﬁﬂKKR
No. 414. Year 1886.
1887.
415
416
417
418
419
420
421
“ﬂax
:..--.=
1888.
1889.
1890.
1891.
1886-91.
1892.
KERR“
aﬁknhnaaa
Mineral Resources Bulletins:—
No. *818. Platinum.
851. Coal.
*854. Asbestos.
857. Infusorial Earth.
858. Manganese.
859. Salt.
Section, 1886. No. 662. Report of Mines Section, 1897.
1887. 698 “ “ 1898.
1888. 718 “ “ 1899.
1889. 744 “ “ 1900.
1890. 800 “ “ 1901.
1891. 835 “ “ 1902.
1892. 893 “ “ 1903.
1893-4. 928 “ “ 1904.
1895. 971 “ “ 1905.
1896.
No. 422. Year 1893. No. 719. Year 1900.
555 “ 1894. 719a “ 1901.
577 “ 1895. 813 “ 1902.
612 “ 1896. 861 “ 1903.
623 “ 1886-96. 896 “ '1904.
640 “ 1897 . 924 “ 1905.
671 “ 1898. 981 “ 1906.
686 “ 1899.
No. 860. Zinc. No. 881. Phosphate.
869. Mica. 882. Copper.
872. Molybdenum and 913. Mineral Pigments.
Tungsten. 953. Barytes.
877. Graphite. 984. Mineral Pigments.
880. Peat.
( French) .
Reports of the Section of Chemistry and Mineralogy:—
No. *102. Year 1874-5.
*110
*119
126
138
148
156
* Publications marked thus are out of print.
KR am
1875—6.
1876—7.
187 7—8.
1878—9.
1879-80.
1880-1-2.
N0. 169.
922
an!
246
273
299
333
359
Year 1882-3-4.
\Kﬁﬁk
unann:
1885.
1886.
1887-8.
1888-9.
1890—1.
1892-3.
616
651
695
724
821
*958
QQRQRQ
No. 580. Year 1894.
1895.
1896.
1898.
1899.
1900.
1906.
REPORTS.
745.
*972.
*260 .
295 .
687.
' 884.
*909 .
943 .
951 .
979 .
982 .
1016.
1050.
212.
*235.
236 .
263 .
*271 .
*294 .
*573 .
574 .
743.
939 .
940 .
986 .
988 .
996 .
1035 .
*237 .
324 .
GENERAL.
Altitudes of Canada, by J. White. 1899.
Descriptive Catalogue of Minerals and Rocks, by R. A. A. Johnston and G. A.
Young.
YUKON.
Yukon district, b G. M. Dawson. 1887. Maps Nos. 274, scale 60 m. =1 in.;
275—277, sca e 8 m. =1 in.
Yukorg and Mackenzie basins, by R. G. McConnell. 1889. Map N 0. 304, scale
4 m. =1 in. =
Klondike gold ﬁelds (preliminary), by R. G. McConnell. 1900. Map N 0. 688,
scale 2 m. =1 in.
Klondike gold ﬁelds, by R. G. McConnell. 1901. Map No. 772, scale 2 m. = 1 in.
Windy Arm, Tagish lake, by R. G. McConnell. 1906. Map No. 916, scale 2
m. =1 in.
Upper Stewart river, by J. Keele. Map No. 938,]
scale 8 m. =1 in. Bound together.
Peel and Wind rivers, by Chas. Camsell. Map N o.
942, scale 8 m. =1 in.
Klondike gravels, by R. G. McConnell. Map No. 1011, scale 40 ch. =1 in.
Conrad and Whitehorse mining districts, by D. D. Cairnes. 1901. Map No.
990, scale 2 m. =1 in.
Klondike Creek and Hill gravels, by R. G. McConnell. (French). Map No.
1011, scale 40 ch. =1 in.
Whitehgtrse Copper Belt, by R. G. McConnell. Maps Nos. 1,026, 1,041, 1,044-
1,0 9.
BRITISH COLUMBIA.
The Rocky mountains (between latitudes 49° and 51° 30°), b G. M. Dawson.
1885. Map No. 223, scale 6 m. =1 in. Map No. 224, sca e 1% m. =1 in.
Vancouver island, by G. M. Dawson. 1886. Map NO. 247, scale 8 m. =1 in.
The Rocky mountains, geological structure, by R. G. McConnell. 1886. Map
No. 248, scale 2 m. in.
Cariboo mining district, by A. Bowman. 1887. Maps Nos. 278-281.
Mineral wealth, by G. M. Dawson.
West Kootenay district, by G. M. Dawson. 1888-9. Map No. 303, scale 8
m. =1 in.
Kamloops district, by G. M. Dawson. 1894. Ma s Nos. 556-7, scale 4 m. = 1 in.
Finlay and Omineca rivers, by R. G. McConnel . 1894. Map No. 567, scale
8 m. =1 in.
Atlin Lake mining division, by J. C. Gwillim. 1899. Map No. 742, scale 4
m.=1 in.
Rossland district, by R. W. Brock. Map No. 941, scale 1,600 ft. =1 in.
Graham island, by R. W. Ells. 1905. Map No. 921, scale 4 m.=1 in., and
Map NO. 922, scale 1 m.=1 in.
Similkameen district, by Chas. Camsell. Ma No. 987, scale 400 ch.=1 in.
Telkwa river and vicinity, by W. W. Leach. IVIap N o. 989, scale 2 m. =1 in.
Nanaimo and New Westminster districts, by O. E. LeRoy. 1907. Map No.
997, scale 4 m. =1 in.
Coal-ﬁelds of Manitoba, Saskatchewan, Alberta, and Eastern British Columbia,
by D. B. Dowling.
ALBERTA.
Central portion, by J. B. Tyrrell. 1886. Maps Nos. 249 and 250, scale 8
m. =1 in.
Peace and Athabaska Rivers district, by R. G. McConnell. 1890-1. Map No.
336, scale 48 m.=1 in.
703 .
949 .
968.
1035 .
213.
601 .
868 .
1035 .
264 .
296 .
325 .
704 .
705 .
1035 .
217 .
238 .
239 .
244 .
267 .
578.
*584.
618 .
657 .
680.
713.
725.
778.
786—787. Grass River region, by J. B. Tyrrell and D. B. Dowling.
815.
819.
905.
215 .
*265 .
266.
3
Yellowhead Pass route, by J. McEvoy. 1898. Map‘No. 676, scale 8 m.=1 in.
Cascade coal-ﬁelds, by D. B. Dowling. Maps (8 sheets) Nos. 929-936, scale
1 'n
m. l .
Moose Mountain district, by D. D. Caimes. Maps No. 963,- scale 2 m. =1 in. ;
N0. 966, scale 1 m. =1 in. ‘
Coal-ﬁelds of Manitoba, Saskatchewan, Alberta, and Eastern British Columbia,
by D. B. Dowling. Map No. 1,010, scale 35 m.=1 in.
~—
SASKATCHEWAN.
Cypress hills and Wood mountain, by R. G. McConnell. 1885. Maps Nos.
225 and 226, scale 8 m.=1 in.
Country between Athabaska lake and Churchill river, by J. B. Tyrrell and
D. B. Dowlin . 1895. Map No. 957, scale 25 m.=1 in.
Souris River coal- eld, by D. B. Dowlin . 1902. _
Coal-ﬁelds of Manitoba, Saskatchewan, Al erta, and Eastern British Columbla,
by D. B. Dowling. Map No. 1,010, scale 35 m.=1 in.
MANITOBA.
Duck anleiding mountains, by J. B. Tyrrell. 1887-8. Map No. 282, scale 8
m. = In.
Glacial Lake Agassiz, by W. Upham. 1889. Maps Nos. 314, 315, 316.
Northwestern portion, by J. B. Tyrrell. 1890-1. Maps Nos. 339 and 350,
scale 8 m. =1 in.
Lake Winnipeg (west shore), by D. B. Dowling. 1898.
M616) N o. 664, scale 8 m. =1 in. Bound together.
Lake innipeg (east shore), by J. B. Tyrrell. .1898.
Ma No. 664, scale 8 m==1 in. '
Coal-ﬁe ds of Manitoba, Saskatchewan, Alberta, and Eastern British Columbia,
by D. B. Dowling. Map No. 1010, scale 35 m=1 in.
NORTH WEST TERRITORIES.
Hudson bay and strait, by R. Bell. 1885. Map No. 229, scale 4 m.=1 in.
Hudson bay, south of, by A. P. Low. 1886.
Attawapiskat and Albany rivers, by R. Bell. 1886.
Northern portion of the Dominion, by G. M. Dawson. 1886. Map No. 255,
scale 200 In. ==1 in.
James bay and countrg east of Hudson bay, by A. P. Low.
Red lake and part of erens river, by D. B. Dowling. 1894. Map No. 576,
scale 8 m. =1 in.
Labrador peninsula, by A. P. Low. 1895. Ma s Nos. 585-588, scale 25 m. =1 in.
Dubawnt, Kazan, and Ferguson rivers, by J. . Tyrrell. 1896. Map No. 603,
scale 25 m.=1 in.
Northern portion of the Labrador peninsula, by A. P. Low.
South Shore Hudson strait and Ungava bay, by A. P. Low. [
Map No. 699, scale 25 m. =1 in. 1\ Bound together.
North Shore Hudson strait and Ungava bay, by R. Bell.
Map No. 699, scale 25 m.=1 in.
Great Bear lake to Great Slave lake, by J. M. Bell. 1900.
East Coast Hudson bay, by A. P. Low. 1900. Maps Nos. 779, 780, 781, scale
8 m.=1 in. 1900
Ekwan river and Sutton lakes, by D. B. Dowling. 1901. Map No. 751, scale
5
0 m. in.
A. P. Low. 1900.
1905.
Nastapoka islands, Hudson bay, by)
The Cruise of the Neptune, by A. . Low.
\
ONTARIO.
Lake of the Woods region, by A. C. Lawson. 1885. Map No. 227, scale 2 m.=
1 In.
Rainy Lake region, by A. C. Lawson. 1887. Map No. 283, scale 4 1n. = 1 in.
Lake Superior, mines and mining, by E. D. Ingall. 1888. Maps Nos. 285,
scale 4 m.=1 in.; No. 286, scale 20 ch. =1 in.
326.
327.
332.
357;
627.
678.
723.
739.
741.
790.
961.
962.
965.
970.
977 .
992.
998.
1075 .
216.
240.
268 .
297 .
328 .
579 .
591 .
670 .
707 .
739 .
788.
863.
. Chibougamau region, by A. P. Low.
962.
974.
975.
998 .
1028 .
1032.
218.
219.
4
Sudbury mining district, b R. Bell. 1890-1. Map No. 343, scale 4 m. =1 in.
Hunter island, b W. H. Smith. 1890-1. Map NO. 342, scale 4 m.=1 in.
Natural Gas and Petroleum, by H. P. H. Brumell. 1890-1. Maps Nos. 344-349.
Victoria, Peterborough, and Hastings counties, by F. D. Adams. 1892-33
On the French River sheet, by R. Bell. 1896. Map No. 570, scale 4 m. =1 1n.
Seine river and Lake Shebandowan map-sheets, by W. McInnes. 1897. Maps
Nos. 589 and 560, scale 4 m.=1 in.
Iron deposits along the Kingston and Pembroke railway, by E. D. Ingall.
1900. Map No. 626, scale 2 m.=1 in.; and lans of 13 mines.
Carligoanuisell, and Prescott counties, by R. W. lls. 1899. (See N O. 739,
ue ec.
Ottawa and vicinity by R. W. Ells. 1900.
Perth sheet, by R. . Ells. 1900. Map No. 789 scale 4 m.=1 in.
Sudbury Nickel and Copper deposits, by A. E. Barlow (Reprint). Maps Nos.
775, 820, scale 1 m. =1 in.; 824, 825, 864, scale 400 ft.=1 1n.
Nipissing and Timiskaming map—Sheets, by A. E. Barlow. (Reprint). Maps
Nos. 599, 606, scale 4 m.=1 in.; No. 944, scale 1 m.= 1 in.
Sudbury' Nickel and Copper degiosits, by A. E. Barlow. (French).
Report on Niagara Falls, by J. . S encer. Maps Nos. 926, 967.
Report on Pembroke sheet, by R. . Ells. Map No. 660, scale 4 m. =1 in.
Report on Northwestern Ontario, traversed by National Transcontinental
railway, between Lake Nipigon and Sturgeon lake, by W. H. Collins. Map
No. 993, scale 4 m.=1 1n.
(French). Map No. 660, scale
Report on Pembroke sheet, by R. W. Ells.
4 m. = 1 in.
Gowganda Mining Division, by W. H. Collins. Map No. 1,076, scale 1 m. =1 in.
QUEBEC.
Mistassini expedition, by A. P. Low. 1884-5. Ma NO. 228, scale 8 m. =1 in.
Compton, Stanstead, Beauce, Richmond, and WO fe counties, by R. W. Ells.
1886. Map N O. 251 (Sherbrooke sheet), scale 4 m.=1 in.
Megantic, Beauce, Dorchester, Levis, Bellechasse, and Montmagny counties,
by R. W. Ells. 1887-8. Map No. 287, scale 40 ch.=1 in.
Mineral resources, by R. W. Ells. 1889.
Portneuf, Quebec, and Montmagny counties by A. P. Low. 1890-1.
Eastern Townships, Montreal sheet, by R. Ells and F. D. Adams. 1894.
Map No. 571, scale 4 m.=1 in.
Laurentian area north Of the Island of Montreal, by F. D. Adams. 1895. Map
NO. 590, scale 4 m.=1 in.
Auriferous deposits, southeastern portion, by R. Chalmers. 1895. Map No.
667, scale 8 m.=1 in.
Eastern Townships, Three Rivers sheet, by R. W. Ells. 1898.
Argentcuil. Ottawa, and Pontiac counties, by R. W. Ells. 1899. (See N o. 739,
Ontario).
Nottaway basin, by R. Bell. 1900. *Map No. 702, scale 10 m. =1 in.
Wells on Island of Montreal, by F. D. Adams. 1901. Maps NOS. 874, 875, 876.
1905.
Timiskaming map-sheet, by A. E. Barlow. (Reprint). Maps Nos. 599, 606,
scale 4 m.=1 in.; 944, scale 1 m.=1 in.
Report on Copper-bearing rocks of Eastern Townships, by J. A. Dresser. Map
NO. 976, scale 8 m.=1 in.
Repo(rlt on h()Jopper-bearing rocks of Eastern Townships, by J. A. Dresser.
renc .
Report on the Pembroke sheet, by R. W. Ells. (French).
Report on a Recent Discovery of Gold near Lake Megantic, Qua, by J. A.
Dresser. Map NO. 1029, scale 2 m.=1 in.
Report on a Recent Discovery of Gold near Lake Megantic, Que, by J. A.
Dresser. (French). Map No. 1029, scale 2 m.=1 in.
. NEW BRUNSWICK.
Western New Brunswick and Eastern Nova Scotia, by R. W. Ells. 1885. Map
No. 230, scale 4 m.=1 in.
Carletonrand Victoria counties, by L. W.Bailey. 1885. Map No. 231, $09.10
4 m.=1 in.
242 .
269 .
330 .
661 .
799 .
803 .
983 .
1034 .
243 .
331 .
358.
628 .
685 .
797 .
871 .
1042.
805.
8 4. Portion of Duncan Creek Mining district, scale 6 m.=1
9 .
916.
990.
991.
1011.
1033.
1041.
1026.
1074
5
Victoria, Restigouche, and Northumberland counties, N.B., by L. W. Bailey
and . McInnes. 1886. Map No. 254, scale 4 m.=1 in.
Northern portion and adjacent areas, by L. W. Bailey and W. McInnes.
1887-8. Map No. 290, scale 4 m.=1 in.
Temiscouata and Rimouski counties, by L. W. Bailey and W. McInnes. 1890—1.
Map No. 350, scale 4 m.=1 in. r '
Mineral resources, b L. W. Baile . 1897. Map No. 675, scale 10 m.=1 1n.
New Brunswick geo ogﬁ, by R. . Ells. 1887.
Carboniferous system, y L. W. Bailey. 1900. I
Coal prospects in, by H. S. Poole. 1900. [Bound together.
Mineral resources, by R. W. Ells. Map No. 969, scale 16 m.=1 in. .
Mineral resources, by R. W. Ells. (French). Map No. 969, scale 16 m. =1 1n-
NOVA SCOTIA.
Guysborough, Antigonish, Pictou, Colchester, and Halifax counties, by Hugh
letcher and E. . Faribault. 1886.
Pictou and Colchester counties, by H. Fletcher. 1890-1.
Southwestern Nova Scotia (preliminary), by L. W. Bailey.
362, scale 8 m.=1 in.
Southwestern Nova Scotia, by L. W. Bailey. 1896. Map No. 641, scale 8
m.=1 in.
Sydney coal-ﬁeld, by H. Fletcher. Maps Nos. 652, 653, 654, scale 1 m. =1 in.
Cambrian rocks of Cape Breton, by G. F. Matthew. 1900. ‘
Pictou coal-ﬁeld, by H. S. Poole. 1902. Map No. 833, scale 25 ch.=1 in.
1892-3. 'Map No.
MAPS.
Dominion of Canada. Minerals. Scale 100 m.=1 in.
YUKON.
Explorations on Macmillan, Upper Pelly, and Stewart rivers, scale 8 m. =1 in.
1n.
Sketch Map Kluane Mining district, scale 6 m.=1 in.
Windy Arm Minin district, Sketch Geological Map, scale 2 m.=1 in.
Conrad and White orse Minin districts, scale 2 m. =1 in.
Tantalus and Five Fingers coa mines, scale 1 m.=1 in.
Bonanza and Hunker creeks. Auriferous gravels. SI ale 40 chains=1 in.
Lower Lake Laberge and vicinity, scale 1 m.=1 in.
Whitehorse Copper belt, scale 1 m.=1 in.
1044-1049. Whitehorse Copper belt. Details.
BRITISH COLUMBIA.
. Cariboo Mining district, scale 2 m. =1 in.
. Shuswap Geological sheet, scale 4 m. =1 in.
. Preliminary Edition, East Kootenay, scale 4 m. =1 in.
. Geological Map of Crowsnest coal-ﬁelds, scale 2 m. =1 in.
. West Kootenay Minerals and Striae, scale 4 m. =1 in.
. West Kootenay Geological sheet, scale 4 m. =1 in.
. Boundary Creek Mining district, scale 1 m. =1 in.
. Nicola coal basin, scale 1 m. =1 in.
. Preliminary Geological Map of Rossland and vicinity, scale 1,600 ft. =1 in.
. Princeton coal basm and Copper Mountain Mining camp, scale 40 ch. =1 in.
. Telkwa river and vicinity, scale 2 m. =1 in. 1
997.
1001 .
1002.
1003.
1004.
1068.
Nanaimo and New Westminster Mining division, scale 4 m. =1 in.
Special Map of Rossland. Topographical sheet. Scale 400 ft. =1 in.
Special Map of Rossland. Geological sheet. Scale 400 ft. =1 in.
Rossland Mining camp. Topographical sheet. Scale 1,200 ft.=1 in.
Rossland Mining camp. Geological sheet. Scale 1,200 ft. =1 in.
Sheep Creek Mining camp. Geological sheet. Scale 1 m. =1 in.
Sheep Creek Mining camp. Topographical sheet. Scale 1 m. =1 in.


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