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GE(

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u

GEOLOGICAL SURVEY OF CANADA

G. M. DAWSON, C.M.G., LL.D., F.R.S., Dibectoh

REPORT

ON THE

GEOLOGY AND NATURAL RESOURCES

OF THK AREA INCLUDE') HY TlIK

NIPISSM AND TEMISCAffllNG mmm

coMpniaiNf; i'ortions of the

DISTRICT or NIPISSmG, ONTilRiO, AIID OF THE COUNTY OF PONTIAC, OUEBIC

ALFRED ERNEST BARLOW, M.A.

OTTAWA

PRINTED BY S. E. DAWSON, PRINTER TO THE QUEEN'S MOST

EXCELLENT MAJESTY

1899

No. 672.

' ' '

ToG:

Sill
featur
Nipiss
Nipiss
accoiu]
constit
series c

flue to

litholog
of man}
critical
for aid (
the dist
Survey,
Palfeozoi

Ackno

l>ee.ston,

power to

Norris, o

Stephen

places or ]

V^. E., engi:

of the Car

of Toronto

of the ioca

informatio

in the vicij

<Jes Peres ;

to Messrs. ,

Lumber Cc

Meteor, and

iscaniing, ai

! I

li!

ToOeorcje M. Dawson, C.M.G., LL.D,, F.R.S.,

Director, Geoloyical Survey of Canada.

Sir, — I beg to transmit herewith ray report on the geoloyy, physical
features and natural resources of the region in the vicinity of Lakes
Nipissing and Tenuscaming, comprising portions of the district of
Nipissing, Ontario, and the county of Puntiac, Quebec. The report is
accompanied by two maps, each on a scale of four miles to one inch,
constituting sheets Nos. 130 and 1.'58, respectively, of the Ontario
series of geological maps.

My gratelul acknowledgments for much kind a.ssistance are
due to Mr. W. F. Ferrier, until lately connected with this Survey as
lithologist, to wliom was entrusted the determination and description
of many of the microscopic sections, especially of .some of the more
critical ones ; to Dr. F. D. Adams, of McGill University, Montreal,
for aid and advice on some points connected with the petrography of
the district ; to Dr. H. M. Ami and Mr. L. M. Lambe, of this
Survey, for their examination of the collections niiide from the several
Palieozoic outliers and the preparation of detailed lists of the fossils.

Acknowledgments are also due to Mr. Colin Rankin and Mr. H. K.
Ileeston, of the Hudson's Bay Company, who did everything in their
power to forward the objects of the exploration ; to Messrs. Frank
Norris, of Baie des Peres, John Turner, ^)i Tomagami Lake, and
Stephen Lafricain, of Bay Lake, officens-in-charge at these several
places or posts belonging to the same company ; to Mr. M. H. iNfcLeod,
vJ.E., engineer-iii-charge of the construction of the Temiscaming branch
of the Canadian Pacific Railway, and also to Messrs. J. C. Bailey, C.E.,
of Toronto, and H. K. Wicksteed, C.E., of Cobourg, enginee».s-in charge
of the location of the projected Nipissing and James Bay Railway, for
information in regard to elevations at various points situated along or
in the vicinity of the lines represented ; to Mr. John Mann, of Baie
des Peres ; to Messrs. C. C. Farr and P. A. Cobbold, of Haileybury ;
to Messrs. J. B. and R. A. Klock, of Klock's Mills ; to the Imperial
Lumber Co., of Warren, Ont.; to Capt. Percy, late of the steamer
Meteor, and Capt. J. O. Blondiii, of the steamer (Jhjde, on Lake Tem-
iscaming, and many others.

! ill

I have the honour to be. Sir,

Your obedient servant,

ALFRED ERNEST BARLOW

NoTK. -y/ie bearin^ throughout this report are yiven itith reference to

the true meridian.

HEPorrr

ON TIIK

CxF.OLOGY A\I) NATURAL RliSOURCHS

OK THE AUEA INCLUDKI* MY TIIK

NIPI8SING AND TEffllSCAMING MAP-SHEETS

COMI'UISINP. POIITIONS OF TIIK

DISI3ICT Of NIPISSING, OITARIO, AMO OF M COUNTY Of POmiAC, OOfBEC.

Introductory.

The following report treats of that portion of the district of Nipiss- position i>f

ing, Ontario, ami the county of Potitiac, Quebec, lying between lati- '''"•^''"^^t-

tudes 4G' llV '2\" and 47' 3()' 47 " north, and extending from longitude

78° 49' o4" to longitude 80' 22' 20 " west of (ireenwich. This area is

comprised in the two maps accompanying the ivport, known as the

Nipissing and Temiscaming sheets, or Nos. 1131 and 138 respectively,

of the Ontario series of geological maps, on a scale or four miles to one

inch. The district which each map represents, measures seventy-two .\,,:i aiid

miles in length from east to west, and forty-eight miles from north to •"""''* "f

south, thus eml)racing an area of 34r)6 s()uare miles, or a combined

area of 0912 square miles. The Nipissing sheet includes nearly the

whole of Lake Nipissing and considerable portions of Dikes Tema-

gami, Temiscaming and Keepawa, the boundary between the two

sheets cutting the three last-named lakes about latitude 46' 55'. The

main line of the Canadian Pacirtc Railway traverses the southern part |{;uiw,ivn.

of the Nipissing sheet, the eastern limit crossing the railway

between Calvin and Eau Claire stations, while the western boundary is

sii/Uated a short distance west of Warren station. The town of North

Bay is the most populous and important place, and is one of the

divisional points on the Canadian Pacific Railway, as well as the '■ini«i;liHii

present terminus of the Northern division of the Grand Trunk Rail- ,, i n/ i
^ ... drniul I milk

way, although the actual intersection of the two lines is at Nipissing Kailway.
Junction, three miles south-east of North Bay. The Grand Trunk

♦j I

MPISSINQ AM) TKMIHCAMIXd KKOION.

lANlOW

AreiiH ill
<.)ueb<'t; aii<l
( )nt»ri<).

by tounnlii|

siirvcVK

NipiiwiiigA Knilwayat prest^ni under tlie title of the Nipissing and James Bay
Hallway, holds a charter for a line to run northward from North
Bay to some point on tlaniew Bay, and already has the road surveyed
and located as far as the eastern extremity of Lake Tcmajnaini. A
portion of the border of the map, near the south-east corner, has been
broken in r rder to show the position of tiie comparatively old and
important town of Mattawa, at the confluence of the Ottawa and the
Mattawa rivers, as well as the junction of the Temiscaming and
Keepawa branches of the Canadian Pacific Kailway.

The Temiscaming sheet contains the northern parts of lakes
Temagami, Temiscaming and Keepawa, and the southern portion of
Jjtic des Quinze. The Ottawa River, from Mattawa to Lac des Quinze,
flows through the region covered by the two maps, the deep-water
channel of this stream forming the boundary between the provinces of
Ontario and Quebec. There is thus an area of about 1 780 square miles
situated within the province of t^uebec, forming part of the county of
Pontiac, while the remainder, 51. ■J2 scjuare miles is included in the dis-
Arttt ijovcicd trict of Nipissing, Ontario. Of the area situated in the province of
Quebec, only about 2<)0 scpiare miles has been surveyed into lots, in-
cluded in the townships of Neudlac, Guigues, Baby, Duhamel, Laver-
lochere, Fabre and Gendreau, bordering on Lake Temiscaming; while in
the province of Ontario an area of about 1911 square miles has been
laid oft' into townships and lots, the greater portion of which (1685
square miles) is contained within the limits of the Nipissing sheet.
The greater number of the townships on the Ontario side are of the
more recent form adopted by the Crown Lands Department of that
province, and measure six miles square, each township thus embracing
an area of thirty-six square miles. Every township is divided into six
concessions by east-andwest lines, run astronomically, which are desig-
nated by the Roman numerals, the order of numbering being from south
to north, while the concessions themselves are subdivided into twelve
lots oy true north-and-south lines, which carry the ordinary Arabic
figures. Each lot therefore measures one mile from north to south
and half a mile from east to west, thus containing a superficies of 320
•acres. Only every altei'nate lot-line is cut out through the bush, the
intervening boundary being simply marked by a post on the concession
line, these being known as " blind lines. " A road allowance occurs
every mile, coinciding with the township, concession, and side lines ;
while occasionally the " blind lines " are utilized for this purpose. The
lines are all supposed to be run astronomically east-and-west or north-
and-south as the case may be, although in some instances no allowance
has been made for the convergence of meridians, thus giving rise

TowuHhips,
howHub-diviil
ed in Ontarin

•ANIOW

INTRODUCTORY.

7 I

to considerable error and confusion. Bordering tlie Mnttawa River
and Lake Nipisaing, as well as on the western shore of Lake Ti'misca-
minf,', the townships are of a somewhat larger size, corresponding in
this respect with those of southern Ontario, while to the south r)f the
Mattawa River, the townships lielong to the older set, both in regard
to size and the direction of their outlines and lines of subdivision.

On the Quebec side, the townships seem to have no regular or slated rowjiHliiiw,
size, and while the hnes are astrononncai, then- direction is determined ,i,.(i ini/uchec.
by the general trend of the water-front. As a conse(iuence, the line.s
of subdivision in the townships of Guigues, Duhamel, etc., are all run
north-and-south or east-and-west respectively, as the upper j>orti(jn of
Lake Temiscaming has, in general, a north -and-.soutli direction, while
the township boundaries and side-lines of Gendreau and other town-
ships situated in the southern part of Lake Temiscaming, have a direc-
tion of N. 60° E. or at right angles to the general trend of the lake
in this vicinity, which is thirty degrees east of south. The distance be-
tween concession-lines is slightly over a mile, but the lots themselves
are much narrower than those on the Ontario side, each being designed
to contain about 100 acres, although in many instances this area is
much diminished or increased. The concessions are denoted by the
Roman numerals, while the ordinary figures are applied to the lots.
Occasionally, both in Ontario and Quebec, the letters of the alphabet
have been used to designate the concessions.

The preliminary part of the work in this district was done in 1887- Wi>rl< '>f'gun
88, while acting under instructions from Dr. R. Bell, as his assistant ; in ih«7.
but only about two months of each season were devoted to this work,
and by far the greater portion of this time was occupied in some of the
many detailed surveys necessary in a region concerning which but
little had hitherto been known. This topographical survey was, of
course, accompanied by as many observations regarding the nature and
distribution of the various rock formations encountered as was possible
in a survey of the kind.

The more pre.ssing nature of the work in connection with the Sud- ^^ '""''^ ""*
bury mining district, caused my removal from this held to assist Dr. Bell
in tracing out the geological and topographical details necessary for
the map and report concerning that region, which has already appeared,
so that work was not resumed on the Nipissing and Temiscaming
sheets till 1892. The bulk of the work on these two maps was accom-
plished between 1892 and 1894, although about two months of the
season of 1895 was required to complete it. It was found necessary
to make a large number of topographical surveys, especially in the

I 1 1

1 \l

i-ii

1 ■/

.;i:^l

8 I

NIIM8SINO AND TKMI8CAMINr. ItKRION.

Mothixt of
Hurvey.

Work
cdnimoiiccd.

KeasoiiH for
<leluy.

Survoy of
Teiiiftjfaiiii
Lak(> I'oinplct
ed in 1HH7.

Survtys ill
1888.

Surveys in
1802-95.

northern part of the district, and this portion of the work occupied hy
far tho <jr«atc'r portion of our time and attention; hut the detailed i-CHults
tlius ohtaine<l have added largely to our g(!0)^raphical knowledge of a
region of which the |)hyuical features were but ru<l(?ly represented, if
at all, on the ina]>8 hitherto published.

The distancen were measured with a Rochon micrometer telescope,
while the direction was determined by prismatic compass. The dis-
tances thus obtained from point to point, were further utilized as bases
for a compass triangulation, by which the position of many of the
smaller islands and some of the more conspicuous points on the main-
land otherwise inaccessible were defined with sulHcient accuracy.
About the middle of .luly, 1887, aj,'reeably with instructions received
from Dr. Bell, then in charge of the work in the district of Nipissing,
r proceeded from Ijake Temiscaming by way of the Matabitcliouan
River and Rabbit Lake to Temagami Lake, in order to complete a de-
tailed topographical and geological survey of that lake. This survey
was commenced on July '23rfl. The work was considerably retarded
owing to the frequent presence of smoke caused by the unusually large
number of l)ush fires, and many days this smoke was so dense as to
render all attempts at surveying quite useless. Another cause which
militated very greatly against the rapid and successful prosecution of
the work during this and succeeding seasons, was the difficulty in procur-
ing and retaining the services of suitabh? canoemen. In spite of these
drawbacks, how«'ver, the survey of Temagami Lake was finished by
September 15th, when a similar survey was undertaken of the route
by way of White-bear and Rabbit lakes and the Matabitchouan River
to Lake Temiscaming. During the summer of 1888, these surveys were
continued, but .scarcely two months of the season were devoted to
field operations in this region. During this time, however, consider-
able progress was made in the topographical measurements of many of
the principal lakes, among the more important of which may be men-
tioned, Cross Lake, the northern part of Obabica Lake, route from the
north arm of Lake Temagami, by way of Red-squ-'^rel and Annima
Nipissing Lakes to Bay Lake on the Montreal River, as well as of many
minor sheets of water to the north and north-east of Temagami Lake.

In 1892, the survey and examination of the Nipissing district was
resumed, with instructions from the Director to make whatever surveys
were deemed necessary for maps, and a report of an approximately
final character. An epitomized statement of the general progress of the
work has been given each year, in which mention is also made of the
various topographical surveys accomplished each season, in the four

•1

RAHI.V KXPLORATIONH AND PIIFVIOUS HHUVEVS.

9 I

Suininnry Itoports of 181)2 to 189').* During 1892 and 180;{, I wiia Ax-i^tMiit^.
ably aHsiuted by Mr. J. K. K. .Johnston, upon whom devolvod the
fjreatflr part of the topo},'rapliical work done during these two years.
In 18.SS, mid again in 189;{ and 1891, I wa.s accompanied hj .Mr. A. M.
Campbell, of Perth. During the .seiuson of 189.S 1 hr.d likewise the
advantage of the assistance of Mr. K. M. Hurwa.sli, of Victoria
University, Toronto.

For cartographical purposes, tlie various bitse, meridian and township Sources of
lines run by the Crown Lands De|)artments of Ontario and Quebec 5'^',f,'Jji^j|!v'ti|*,,
have been utilized, and servo as excellent checks and corrections to
the errors necessarily incident to a micrometer and compass survey.
The geographical features of the area covered by the .surveyed town-
ships have, in the main, been adoptei], supplemented, however, in many
cases by additions and corrections of our own, wiiich were sometii\iea
found neces.sary. This information was chietly availal)le in the area of the
Nipissifig sheet, where over half tlie area has been divided ' 'o town-
ships, and these in turn subdivided into conce.ssions ind lots. sides
these a luimber of surveys of a more general character h i\ > been
made, the maimscripts and published plans of whid. have been
found of much aissistance in the general compilation, as well as iu
furnishing details !i many cases not otherwise obtainable. "niong SurvtyH l>.v
the more important of these plans, the following may be iiicniioned : V|If,""y"'
Murni. .survey of Lake Nipissing and the 8turgecn River, and
Logan's survey of the Mattawa River, published in the folio atlas to
accompany the Report of this Survey of ISoiJ-nG. Murray's survey of
Lake Nipissing, however, did not show sutiicient detail in the western
portion of the lake, so that a resurvey was carried out early in 1892.
Austen's map of the Temagami River, with accompanying traverses
made for the purpose of ascertaining the most feasible route for the
location of a transcontinental railway line, h'orrest's survey of the l". uroHt'H
Montreal River was found excellent for all purposes for which it was
required. Messrs. O'Dwyer and O'Hanly's survey of the Ottawa oDwytr'sixnd
River and Lake Temiscaming, to delineate the boundary line between j^'irvl-vs^ ^
Ontario and Quebec, was found to be thoroughly reliable, while the

Canadian Pacific Railway surveys enabled us to locate the exact <'iinii<liiiii

,. I'uciHcRy

position of the railway line. surveys.

Early Explorationa and Previous Surveys.

The history of the exploration of the region in the vicinity of the | ji^trict early
Upper Ottawa and Mattawa rivers, dates back almost to the first l^""""-

• Huminary Rbiwrt, Geol. Surv. Can., 1892, Part A, pp. 34-35. 1893, Part A, pp.
30-33. 1894, Part A, pp. 55-57. 1895, Part A. pp. 61-63.

fi'i'i

10 1

NIPISSING AND TEMI8CAMING REOIOV.

settlement ot Canada by tho French. Tlie almost invariable presence
of detached parties of tlie war-like and much dreaded Iroquois in the
region immediately adjacent to the upper Hi. Lawrence, uisually for-
bade the utilization of th' ' main artery as a route towards the west,
so that in most instances the more peaceable, though more circuitous,
passage by way of the Mattawa and the upper Ottawa River was the
only practicable channel of communication between the scattered
French settlements on the Lower St. Lawrence and the populous
villages of the Hurons and other friendly Indian tribes inhabiting
the region in the vicinity of (.Jeorgian Bay and Lake Simcoe.
It is therefore not .surprising to find that the various physical features
presented in the regions in the vicinity of these streams were at a very
early date among the best known, being especially familiar to the mis-
sionary and fur-trader, whose avocations forced them to make constantly
recurring visits to the outposts already established in the distant west
and northwest. Tho most prominent of these geographical features were
appropriately designated, and most of the names then bestowed upon
the numerviiis rapids, portages, etc., are still retained in common use
throughout the district.

Miittiiwn
route, wliy
Mtilizpil.

Proi>osMl
canal.

CJhaiiiiilaiii':
journey
in 1012.

Nicolas
du Vignau.

The sheltered nature of its water-stretches, its comparative freedom
from molestation, as well as its directness as a route to tlie great lakes
and bsyond, formed powerful inducements in favour of the original
selection of the Ottawa and Nipi.ssing route, at a time when the birch-
bark canoe was the chief and often the only method of communication.
The advent of steamboat navigation on tho St. Lawrence River and
the great lakes, however, as well as the building of the St. liawrence
canals, have during the present century caused this route to fall into
comparative disuse. The recently revived proposal to make use of these
water-courses for purpo.ses of modern navigation by the building of
canals to overcome the obstructing rapids, seems likely again to bring
this district into prominence.

Soon after his arrival in this counti-y, Samuel de Champlain, who was
by nature more of an explorer and adventurer than a builder of colonies,
determined on an examination of the head-waters of the Ottawa and
beyond. He was all the more eager to undertake this investigation as
a young man, Nicolas du Vignau, had just returned, in 1612, after a
year's absence among the Ottawa Indians, with a most wonderful tale.
He claimed, during his absence, to have discovered a passage by way
of the Upper Ottawa to the shores of a northern sea, to whicli he had
penetrated, and there beheld the wreck of an English ship. The
apparent clearness and consistency of the story deceived Champlain,

KARLY EXI'LOHATIONB AND PUEVIOUS SURVEYS.

11 I

who fancied that he might thus find tlie much coveted road to China and

Japan. Towards the end of May, 1613, Champlain, accompanied by ciiamplain's

this Du Vignau, ascended the Ottawa as far as Lake Coulonge, where ""^'^ "'"

he was reluctantly dissuaded by the resident natives from proceeding

further. They urged, as their main excuse for not seeming willing to

guide him, the many insuperable difficulties to be encountered on

the route, as well as the reputed fierceness and witchcraft of the Nipiss-

ing IndianS; through whose country it was necessary to pass. Here also

he learned that tiie whole story of Du Vignau's pretended discoveries

was a fabrication, and that far from undertaking any such important

journey as reported, h^s had resided continuously and (juietly at the

village during the entire period of his absence from civilization. This

information, which was subsequently corroborated by Du Vignau's own

tardy confession, enraged and disheartened Champlain, who, convinced

of the fruitlessness of any further effort at the time in this direction,

returned to Montreal, and subsequently to France.

Early in 1615, however, Champlain returned to Canada, bringing ciuvniplain's
with him four Recollets, one of whom Father Joseph Le Caron, was •■^l'|<>''ations
destined for missionary work among the Huron Indians. Arriving at Arrival at
Montreal, he found a large concourse of Indians already assembled, who Mi'iifeal.
had come hither from their homes in the vicinity of Lake Simcoe.
These savages, always more eager for temporal than spiritual help,
again pressed Champlain to aid them against their hereditary foe, the
formidable Iroquois Deeming it expedient at the time to comply with
this oft-repealed reijuest, Champlain hurriedly descended to Quebec to
make the necessary preparations, leaving Le Caron and some of his
compatriots with the assembled Indians to await his return. During
Champlain's absence, however, the Indians decided to go back forth-
with to their ov/n home without him, and accompanied by Le Caron
and his associates commenced the ascent of the Ottawa River. When
Champlain returned to Montreal and found the place deserted, he Ui^coviry of
immediately hurried after them, pursuing the usual course up the \i,ii!!gi,i„ j,„rt
Ottawa and Mattawa rivers, over the height-of-land to Lake Nipiss- Huron,
ing and tlience down the French River to Lake Huron. Champlain
was thus the first European, with the exception of the humble friar
who had only just preceded him by a few days, to gaze on the waters
of Lake Huron, which ho christened " Mer Douce."

J ■ f .

Champlain's map of New France, which was made in 1632, included ciiampliun's
all sketches and surveys from 1603 to 1629. Only th<; main routes ot ""*''•
travel are represented, while the whole map exhibits, in a very rough
manner, the salient physical features encountered during the progress

12 I

NIPISSINO AND TEMISCAMINf} RErilON.

Exploratiiiii
clfist'ly con-
nected with
fiirtradp.

of theso journeys and explorations. Lake Nipissing is called "Lac de
Biserinis " while a rude outline of the Ottawa River ahove its confluence
with the Mattawa is given, that must have been drawn from infor-
mation supplied by the Indians.

The exploration of this district, as of others elsewhere through-
out Canada, is inseparably bound up with the history of the fur-trade,
the successful prosecution and extension of which required the constant
addition of new territory. We thus find that many of the first ex-
ploratory expeditions wero often undertaken by adventurers at their
own expense, with the promise of various marks of distinction from
those in authority in cjuse of the success of their undertakings, while
fur-trading licenses were granted to enable these men to indemnify
themselves for their pecuniary outlay.

Delisles iii!i|p '^he limits of this traffic were quickly extended both northward and

andiKwitioiM.f westward, and we find by reference to Delisle's map (1703) that the

Fort des ^ ■'^ _ _ , , .

Abitibis. French then had a post (Fort des Abitibis) north of the height of-land

on the river Abitibi. This post, according to the memorial of Begon*
was the most advanced station of the Fnnch toward Hudson Bay.
From this same memorial, it also appears certain that the route north-
ward by way of Lake Temiscaming and the Abitibi River (Monsony
or Monsipy) was one of the best known, although the French traders
avoided the immediate vicinity of Hudson Bay in order not to expose
themselves to the insults of the Indians who were friendly to and
traded with the English posts already established in that vicinity. It
Exiwditidiis to does not seem unreasonable to suppose, therefore, that some of the ex-
peditions despatched by the Governors of Cancada towaril the close of
the 17th century, to take possession of Hudson Bay, adopted this well
known route by way of the Upper Ottawa and Abitibi rivers. All the
earlier maps indicate many of the streams flowing northward from the
height-of-land into James Bay with tolerable accuracy, thus showing
that the early voyageurs were well acquainted with this portion of the
country.

Hiidaon l>!iy
towards tlic
closfi of ITtli
century.

Fort Teiiiiscii
niini< early
e8tai)lisli('d.

Fort Temiscaming must have been one of the first posts established
by the Northwest Company, if not acijuired after its abandonment by
the French, for Mr. Roderic Mackenzie, a clerk in this company who
wrote" A General History of the Fur Trade,' which forms the opening
chapter of Sir Alexander Mackenzie's Travels in North America says :

*Menioire de Eegon, Oct. 20 1725, qui expli(iue lea anciennes lin'ites du poste
de TeniiscaminiTue.

fVoyajjes from Montreal throufirh the Continent of North America to the Frozen
and I'acific Oceans in the years 1789 and 1703. London, 1801. p. xxxiv.

•J

KAHLY EXPLORATIONS AND PKEVIOl'S SURVKYS.

13 I

" Lake Teiniscaniing wliero there has always been a trading post " Miuki'ii/ic's
while one of the buildings which had lieen used as a store-house and "'^'' *"
which was removed only a few years ago, bore dates on the large
cedar beams wliicli pointed to its erection some time near the close of
last century.

Fort Temiscaming afterwards became the liead-quarters of the Utadquintirs
Hudson's Bay Company in tliis district, containing the residence of the j'j jj (^•^^
Chief Factor and all the necessary adjuncts in the shape of buildings,
etc., which usually go to make up a well equipped establishment, form-
ing one of the most impui-tont centres of the fur trade and containing
besides a library embracing many volumes on science, travels and gen-
eral literature. In 1888, however, this post, so long established, was iJ'inovnl
abandoned, and a small store was erected at "The Point" near the '
village of Baie des Pisres, which was found more convenient for purposes
of general trading ; while the opening,' up (»f the Canadian Pacific Rail-
way had previously caused tile removal of the iiead-tiuarters to
Mattawa.

Temagami post, now situated on the west side of Bear Island <m r, maKaini
Lake Temag.imi, was movetl to its present site in 187rt, on .account of j"'";' "i"^'''
the opening of an opposition fur-tiading establishment, owned by
Alexander Dukis, who soon left his stronger rival in undisputed posses-
sion of the place. Before its removal thence, this post was located
on the shores of a small cove on the south side of Temagami I-^land,
and ruins of the buildings are still visible at this place. Fort Wrath, |.-,„.t Wmtli.
of which the tumbled-down buildings may even now be noticed on the
east shore of Lake Temiscaming, about a mile above Piche Point,
was built to overcome the rival post operated by Mr. Piche, who still
resides at his farm on the point which bears his name. This place
was kept open for a few years onl}', when the necessity for its pres-
ence ceased. The somewhat important post near the mouth of the stur^'ion
Sturgeon River, continued actively engaged in trade with the Indians 1!'\<> !"»♦'•
until the opening of the railway, when it gradually* fell into disuse and
was finally abandoned altogether about the year 1890. Hunters HnntetK
Lodge, originally a trading establishment, situated on Hunters ''"''^"'■
Narrows in Keepawa Lake, was abandoned about the same time. At
several points on the Ottawa River and the lower portions of Lake
Temiscaming, temporary posts were erected from time to time,
but these were of no permanent importance, and when the reasons
which brought tiiem into existence disappeared, they were given up
and forgotten. Buildings originally erected in 1887, and designed for i5ayi,Mi<|.,,(ist.
storage purposes on liay Lake, an expansion of the Montreal River, have

i iif

! ( i

i" ? ;

i^i.

14 I

MPISSINfJ AM) TKMI.SCAMING REGIOX.

Lon^ Point.

Decrt
fnr-trafle.

nst' III

since been raised to the dignity of a post with an ofticer in charge.
At present, in the area of the accouipanying map-sheet.s, there are only
three cstahlishment.s, Temaganii, Bay Lake and Long Point (on
«' Quinze Lake "), which receive any gi eat quantity of fur.s, although a
considerable number of skins come in casually to the posts at Mattawa
and Baie des Peres during each year. Of these Temaganii is the most
important, but the gradual opening up of considerable areas in this
district to settlement, and the diminution in point of number both of
the fur-bearing animals and the Indians who are chiefly engaged in
their capture, is already having a marked effect, showing a gradual,
or in some cases a rapid decrease in the number of skins annually
brought to market.

The opening chapters ot ]Mackenzie's narrativf, previously mentioned,
give a lirief description of the route generally pursued by the fur-
trading canoes in gaining access to the various forts and trading posts
of the inteiior. The i-apids and portages of the Mattawa are enum-
erated, the names in most cases being the same as those in use at the
present time, although the river itself is here called Petite Riviere.
Nepisingui (Nipissing) Lake is also mentioned, and a short account
given of the Riviere de.s Francois.* The first geological account of the
Work liy I )r. region in question was that of Dr. J. J. Bigsby, who had come to
ill IS-.'o. Canada as medical officer to a regiment. About the yeai- 1820, he

received an appoirtment from the Colonial Government to make a
generid report on the geology of Upper Canada, the absurdly small
sum of twenty-six pounds, as he informs us, being granted as pecuni-
ary aid to carry out this extensive undertaking. Dr. Bigsby lirst
made an examination of the Ottawa, Mattawa and French rivers, to-
gether with Lake Nipissing, having been granted a free passage to
Sault Ste. Marie in one of the Northwest Company's canoes. He gives
a good account of the Ottawa River itself and of the country adjoin-
ing this stream, and mentions that the Mattawa River, which was
the western branch of the Ottawa, often called the Little Ottawa, was
known as the Tessouac River by the Indians. The occurrence of
crystalline limestones at the Talon Chute is noticed, among other inter-
esting facts. The position of " La Itonde," a Northwest Company's
post, is noted as being situated at the mouth of the Vase River, as
well as its subsequent removal to one of the islands in Lake Nipissing. t

Cry-iriiiliiii'

lilllCStKllCH Mt

Talon Cluit)'.

nia>fiieti(

During the pR)gress of the magnetic survey of British North
America, executed between 1842-1844 by Sir J. H. Lefroy, various

* See |i]i. xxxiv. anil xxx\. MackMi/.ie'M Voyages.

t Shoe and Canoe, vol. 1. London, 1850. pp. 105 to 171.

formations

•]

EAHLY KXPLORATIONS AND I'KEVIOUS SUfiVEYS.

l.-) I

observations were taken in this rej^ion to ascertain tlie magnetic varia-
tion, 'vhile latitudes were obtained at the following places : Hudson's
Bay Company's post Mattawa, First portage on Little (Mattawa)
River, Lake Teinisiquc (Lower Trout Lake); Lake do Talon or Lake
Walrond ; Trout Lake, formerly called Lake de Grande Vase ;
Height-of-land portage, towards Lake Nipissing ; and Cross Point
on the south shore of Lake Nipissing, where a cross had V)een
erected to commemorate some fatal accident.*

For many years the region in the vicinity of the Upper Ottawa U|i|"r<)tt!i\v;i
IT • 1 1 1 • 1 ^ II "listrict

Kiver was comparatively unknown, except to the occasional traveller ,,,niiia',ai\fly

and missionary, and to those engaged in the fur-trade, whose business "'"^""">'-
necessitated constant journeying to and fro along the main canoe-
routes. Tn time, however, the almost inexhaustii)le supply of valualjle
timlier known to exist in this district, attracted the attention of the
enterprising lumberman, wlu)se operations were so ((uickly extended IjuniiHiii!.,'
north-wc'sLward that, by the year 1 f<io, we find that lumber camps were " ^
in full operation in the vicinity of the Opimika Narrows (the "Galore")
while some two or three years previously, red pine timber had
been cut on Lake Temiscaming several miles above the Narrows at the
Hudson's Bay Company's post. These lumbering outposts, however,
were for the purpose of cutting red pine alone, the value of
which at this time caused it to be sought for at greater distances than the
white pine ; for previous to this no white pine had been cut higlier
than Bennett Brook on the Ottawa River.

The first really accurate delineation of the topographical features NN'mk hv Sir
within the area comprised by the two accompanying map-sheets, was '"" " *"K""'
made by Sir William E. Logan, the founder and first Director of the
Geological Survey of Canada, in the year 1845.f

A geological section across the western part of Canadii, from Lake ll.asoiis fcir
Huron to Lake Erie, iuiving previously been made by Mr. Alexander ( iitaVa Hiv. r.
Murray, in 181.!, in addition to an examination into the stratigraphiciil
relation of the rocks comprising the extreme eastern portion of Can-
ada, by Sir William Logan himself, it was considered expedient that
a third section should be undertaken across and embracing some part of
the northern district. The Ottawa River was chosen, for various
reasons, the chief of which was perhaps its accessibility and the greater
immediate utility to the country at large which such a survey promised.
Starting from Montreal, ho made an examination of the various rock
formations exposed on the shores of the Ottawa, taking occasional short

* See Lufroy's Magnetic Survey of the Dominion of Canada. London, 1883.
t Report of Frogrres.i, (Jcol. Surv. Can., 1845-1().

i-'i

16 I

NIPI88ING AND TKMI8CAMINO REGION.

excursions inland wherever deemed necessary. This geolo;»ical inves-
tigation was continued as far as the mouth of Bennett Brook, about
T()i)o>riYi>hi(ivl five miles above the "des Joachim " liapids. As this was the highest
at Heniu'tt point yot reached in the topographical delineation of the course of the
BnK.k. Ottawa, it was decided to make this the starting point of the contem-

plated survey of the upper portion of this stream. The distances were
determined by the Rochon micrometer telescope, while the bearings
and angles of intersection wore obtained by means of a theodolite.
The diflFerences in level of the river at all the rapids were ascertained
by careful levelling with a proper instrument and stall', the fall in the
intervening stretches being estimated from a knowledge of the strength
of the current. This survey was continued up the Ottawa as far as
the first chute on the llivii-re des Quin/.e, a short distance above the
head of Lake Temiscaniing. During the same season, and as a
necessary adjunct, a similar survey was undertaken of the Mattawa
River, from its junction with the Ottawa to its head-waters in Trout
Lake, including also the portage-route by way of the Riviere de la
Vase to Lake Nipissing, as well as a small portion of the shore-line of
this lake in the vicinity of the mouth of this inlet. Observations for
latitude were obtained at the starting point, the mouth of the Mat-
tawa, the mouth of the Vase on Lake Nipissing, as well as
at the mouth of the Keepawa on Lake Temiscaniing. In fact,
every precaution was taken to make this survey as accurate as was
possible with the instruments and time at his disposal. The various
topographical details, delineated in a map subsequently compiled by
Sir William Logan himself on a scale
bearing valuable notes regarding the

encountered, is at present on file at this office, and although not issued
as a separate publication, the information has been made use of in
every subsecjuent map covering the district.

Survey to
i.^uiiizf KivtT.

Survey of

.Matt;nv;i

Kiv.T.

I>(i0iilitifs (1
.ili>;t'r\:itiiiu
fi»l- livtitiidf

Miip l.y

Murniy'^
sur\cvs \n
ISairiC.

of one

various

mile to an inch,
rock formations

A portion of the Ottawa River in the neighbourhood of the Mattawa,
as well as the whole of this latter sti-eam, were, however, incorporated
in the atlas to accompany the report by Mr. Alexander Muriay
(1853-56). During the summer and autumn of 1854, Mr. Alexander
Murray, of this Survey, was engaged in making exploratory surveys to
the east of Lake Huron and Georgian Bay. These included a survey
of the southern shore of Lake Nipissing, from the point where the
French River measurement ceased in 1847, to the mouth of the Vase,
where connection was made with Sir William Logan's survey of 1845,
and thence of the north shore, of this sheet of water toils "north-
west angle."* In 1855, Mr. Murray continued this survey, commenc-

• Report of ProgreeB, Geol. Surv. Can., 1853-56, p. 101 et seq.

EARLY EXPLORATIONS AND PREVIOUS SURVEYS.

17 I

Surveys i>f
Luke.

ing at the outlet of Lake Nipissing into the French River, along the
western coast making connection with the work of the previous year.*
In 1856 this survey was again extended, this time a start being
made from the Hudson's Bay Company's Post on Sturgeon River
near Lake Nipissing.

Ascending the Sturgeon River for about fifty-two miles to the moutli
of the Maskinonge, the measurements were carried up this important
branch through Murray, Washkigamog, Maskinong^-wagaming and
Mattagamashing lakes to Wahnapitae Lake, and down the Wahna
pitae RivT to Lake Huron.f

In 1855, Duncan Sinclair made a survey of Keepawa Lake, with a
view of defining and locating certain timV)er limits. This survey,
although excellent for the purpose for which it was undertaken, never-
theless lacked certain details essential for a correct elujidation of the
geological features, thus necessitating a re-survey v/hich was accom-
plished by Mr. J. F. E. Johnston, of this Department

Acting under instructions from the Commissioner of Public Works, Canal surveys.
Mr. M'^alter Shanly, C.E.J in 1856-57 made » ueiailed examination of
the route contemplated for a canal to connect the waters of the St.
Lawrence with those of the Great Lakes by way of the Ottawa,
Mattawa and French rivers, and Lake Nipissing.

In 1858-59, another examination of the same route was made by
Mr. T. C. Clarke, C.E.,^ also in accordance with instructions received
from the Commissioners of Public Works.

In 1867, Mr. A. G. Forrest, acting under instructions from Forrest's
the Crown Lands Department of Ontario, made a survey with transit «»""^';y "f
and chain of the Montreal River, starting from its intersection with a Kivcr.
due west astronomical line, supposed to be run on the parallel of latitude
of 47°56', between Michipicoten Harbour on Lake Superior and the
head-waters of the Montreal River. This astronomical line was started
about the same time from its eastern and western extremities. Mr.
Duncan Sinclair who was entrusted with the eastern portion of the
line succeeded in running a distance of 105 miles from the Montreal
River, while Messrs. A. P. Slater and R. Gilmour, ran eighty-

; i t-

' 'I

u t

.Vstronoiiiical
line.

*ReiK)rt of Progress, Oeol. Surv. Can., 1853-56 pp. 128 and 135 et seq.

+Report of Progress, Oeol. Siirv. Can., 1853-.56, pp. 146 et sef).

JRejwrt of Walter Shanly, Esq., On the Ottawa Survey,— Toronto. March
22nd, 1858. Also Report on the Ottawa and French River Navigation I'roject, —
published by order of the Montreal Board of Trade, 1803.

§ Return of Recent Survey and Report of the Engineer on the Ottawa Ship
Canal Quebec, 1860 by Thos. C. Clarke, C.E.
2

:i'!.

18 I

NIPI88ING AND TEMI8CAMINO REGION.

ForrestV
work.

fiiii

HP
I"

Traverse liy
Lindsay

RUHS€!11.

Surveys tiiulcr
Mr. Rowan.

Work by W.
McOuat.

Survf^y of

four miles eastward from Michipicoten Harbour. Mr. Forrest, from
the intersection with Sinclair's line made an instrumental traverse of the
Montreal River to its mouth on Lake Temiscaming, a distance of one
hundred and one and a quarter miles, at the same time taking notes on
the timher and other natural resources of the country extending for
three miles on either side of the stream. These surveys, commenced in
1866, were completed in 1867. Their primary object seems to have been
to determine the feasibility of the construction of either a wagon road
or railway to the Red River country through the district in question.*

About the same lime (June 13th to August 16th, 1867), Mr. Lind-
say Russell, made a micrometer traverse of Lac des Quinze and
the Upper Ottawa, connecting with H. C. Symmes' survey of
Grand Lake. Mr. Russell during the same sei.son made a similar
survey of the route to Lake Abitibi, as well as a traverse of this large
sheet of lake, then for the first time correctly measured.!

In 1871, Mr. Alexander McKenzie, acting under instructicms from
Mr. James H. Rowan, who hud charge of the Canadian Pacilic Rail-
way surveys from the Mattawa to the Red River, made a track-survey
northward by the Ottawa and Abitibi rivers to James Bay, returning
by way of the Moo.se and Michipicoten rivers to Lake Superior. J

In 1871-72, Messrs. Lloyd, O'Hanly and Austen, also under Mr.
Rowan's instructions, made exploratory surveys from Mattawa by way
of the Ottawa and Montreal rivers to a point about half-way between
this latter stream and one of the branches of Moose River. §

In 1872, Mr. Walter McOuat of this Survey was engaged
in a geological examination of that portion of the country to the north
and east of Lake Temiscaming. The work performed by Mr. McOuat in
the Temiscaming region embraced a most painstaking geological exam-
ination of Rivifere des Quinze, Lac des Quinze and the route thence
northward to Lake Abitibi, including a micrometer survey of the shores
and islands of that lake. He also made a micrometer traverse of

BlanclieKiver. (;j,p Blanche River as far as Round Lake, accompanied by an examina-

*See Remarks, on Upper Can.ada surveys, 1867 ]>]>. 6<)-02.

tSee Reix)rt Cominissioner of Crown Lands, (juel)ec, 18G8, p. XVII, also descrip-
tions of the Surveyed Townshiiis and Territories of the province of Quebec, 1889, pp.
416-424.

+See Progress Retwrt on Surveys Canadian Pacific Railway, 1872 p. 74.

Also Report on Surveys Canadian Pacific Railway, 1877, pp. 5-47 and 48.

§ See Progress Rejwrt on Canadian Pacific Exploratory Surveys, 1872. These
surveys comprised Divisions B, C and D, re8i)ectively, mentioned in these reports.
The surveys were begun on June 10th, 1871, and the last of them was completed by
July, 1872. See also Report on Surveys, Canadian I'aei fie Railway, 1877, pp. 5 and 47.

tion
to ac
conta
embn

•AMIOW

]

EARLY EXPLORATIONS AND PREVIOUS 8DRVET8.

19 I

tion of the rocks in the immediate vicinity of this stream.* The plans
to accompany his report have never been published, but the information
contained has been utilized in subsequent general geological maps
embracing this area.

In 1872-74, Messrs. O'Hanly and O'Dwyer, joint commissioners for l'n>vincial
^ . , -, , , . J ' ■) lioundary

Ontario and Quebec, made an instrumental traverse of the Ottawa siirvcy.

from Mattawa to the head of Lake Tomiscaming, and .surveyed a line

running northward from a point on the " Chenail du Diable," near

the mouth of the Riviere des Quinze as far as the height-of-land.t

During the year 187G, in connection with the location of the Canadian ^ • •'• H.

8UrV6V9

Pacific Railway, Mr. Marcus Smith, then acting engineer-in-chief,
made an examination of the eastern portion of Lake Nipissing, as well
as of the " Beuve" (Veuve) River as far as the forks, about twenty-
five miles from the mouth. t

In 1879, Mr. W. A. Austen, for the Canadian Pacific Railway, ran
a trial location survey from a point situated a short distance (404 feet)
east of the deep-water landing at South-east Bay (or East Ray) of
Lake Nipissing, in a north-easterly direction for sixty-three miles up
the valley of the Sturgeon River.g As a part of the same survey,
Mr. Austen made a micrometer survey of the Temagami River, the
southern portions of Cross and Temagami lakes as well as the route
from thence to Maskinong^-wagaming Lake, by way of Obabica and
Wawiagama lakes.

During the summer of 1884, commencing in June, Mr. T. Guerin, Gnerin's
engineer of the Public Works Department, Ottawa, undertook an '
examination of the Ottawa River and Lake Temiscaming with a view
to ascertaining the feasibility, at a reasonable cost, of the various
schemes urged on the Government from time to time, looking to an
increased facility in the navigation of these waters.||

In the summer of 1884, Dr. Selwyn, during the progress of an Work by

examination of the numerous rock-cuts exposed along the line of the

l)r. Selwyn,

•Report of Progress, Geol. Surv. Can., 1872-1873 pp. 112 et seq.

t The manuscript plan of a scale or 40 chains to one inch beari; the date, Dec.
27th, 1875, while the joint report filed vvitii the Crown Lands Department, is dated
Ottawa, Dec. 7th, 1874.

+ Report Canadian I'acific Railway, 1877, pp. 359-3()().

§ Appendix 18, "Reiwrt Canadian Pacific Railway, 1880, pp. 290-296." A plan
on 4000 feet to an inch, detailing these explorations, as also two jirofiles of the
Sturgeon River are on file at the Deiiartment of Railways and Canals, Ottawa, and
have been of much assistance in the compilation of the accompanying maps.

i Ann. Rep. Minister of Public Works, 1884-85, pp. 103-124.

20 I

NIPISSINr. AND TEUI8CAMINO REOIOK.

KossIIh.

\i: :i

Kxaiiiiiiatioii
by Prof. C.
K. (JillHi-t.

Prof. Wright';
observatiun.-i.

F. H. Taylor's
observations.

Canadian Pacitic Railway, paid a visit to the Manitou Islands in Lake
Nipissing, and the Ii.st of the fossils then collected from the Canibro-
Silurian outliers comprising seventeen specie.s, together with a few
notes regarding their occurrence was published by Dr. H. M. Ami*.

The Rev. J. M. Goodwillie, who was stationed at North Bay for some
years, has made an extensive collection of the fossil remains from these
islands, and these have now been examined and their identification
has greatly iulded to the list appended to this report.

Mr. Ulrich determined a small collection of fossils for Professor N.
H. Winchell, which were collected by Mr. T. D. Ledyard, of Toronto.!
In 1889, Prof. N. H. Winchell paid a visit to North Bay, and gives a
record of his observations made in that vicinity. |

In 1889 Mr. G. K. Gilbert made an examination of the vicinity of
North Bay and the country eastward-^ towards Mattawa, with a view
to obtaining any evidence regarding the former existence of T.n out-
let for the Great Lakes, immediately following the retirement of the
ice-sheet. The possibility and even the probability of the existence of
.such an outlet had been looked upon for some time with favour by
.some geologists, although facts in support of these views were not
forthcoming previous to the communication made by Mr. G. K. Gilbert
to the meeting of the American Association for the Advancement of
Science, held in Toronto in August, 1889. The general sub.stance of
the remarks then made were published under the title of "The History
of the Niagara River. "§

In Soptemlier, 1892, Prof. G. F. Wright visited the neighbourhood
of North Baj- and Mattawa, making certain observations seemingly
confirmatory of the former existence in the Mattawa valley of this
outlet, and embodying the results of his observations in a paper
entitled, "The Supposed Post-glacial Outlet of the Great Lakes through
Lake Nipissing and the Mattawa River." ||

In the autumn of 1893, Mr. F. B. Taylor made some observtvtions
in regard to the occurrence of beaches in the vicinity of North Bay,
and their relations to this supposed old outlet of the Great Lakes.

* Can. Rec. Science, April, 18f)2, pp. 108 ot seq.

+ American fJeologist, vol. XVIII., No. 3, September, 1896, p. 178.

+ EiRliteenth Annual Report, Geol. and Nat. Hist. Survey, Minnesota, 1889,
p. 501.

§ Sixth Annual RejHjrt of the Commissioner.s of the State Re.servation at
Niagara for 1889, pi>. (il-84, and reprinted in the Smithsonian Report for 1890, pp_
231-2.57.

i Bull. Geol. Sec. Am., vol. IV., 1893, with discuasion by Dr. Robert Bell,
pp. 423-42(>.

•'

•ARkOW

OENEKAL PHYSICAL FEATURES.

21 I

The results then obtained were communicated to the (Jeologioal Society
of America, and published in the bulletin of that society.* In 1895,
another visit was paid to the Nipissing District with the similar object
of gaining additional information in regard to the recent changes of
level, t

In 189(5, a third visit was paid to the region in tlie neighbourhood
of the Mattawa and Ottawa rivers, and the results then obtained
were communicated to the Geological Socifty of America.

In 1890, William Ogilvie, acting under instructions from the Depart- I,;ititu(l« und
ment of the Interior, Ottawa, fixed the latitude and longitude of ^I';^naw'll! '
Mattawa, the latter by telegraph from Ottawa.

In 1892, Messrs. H. K. Wicksteed and Patterson, under the direc- Siirve>;8()f
tion cf Mr. J. C. Bailey, C.E., of Toronto, made the location ,'i.i„'iesi5(iyRy,
survey of the Nipissing and James Bay Railway from North Bay
to the North east Arm of Lake Temagami. INIr. Patterson had
charge of the location of the southern portion of the line from
North Bay to Marten Lake, and Mr. Wicksteed of the northern
pare.

The building of the Temiscaming branch of the Canadian Pacific Surveys by M.
Railway and the surveys and levels made in connection therewith,
have been used in the present map and report, the information being
kindly supplied by Mr. M. H. McLeod, the engineer-in-charge.

General Pliysical Features.

The generial character of the country may perhaps be best described (jentral
as that of an uneven or undulating ro^ky plateau, with a gentle slope t'luiracter of
towards the east and south-east. Although in detail the surface of
this plateau is far from uniform, consisting of a succession of more or
less parallel rocky ridges, with intervening valleys occupied by swamps
or lakes, still the district as a whole has a general elevation
varying from 900 to 1200 feet above the sea. There are no very
prominent hills, the highest seldom attaining a greater altitude than
300 feet above the surrounding region, while throughout most of the
district, hills of 50 to 100 feet in height are rather conspicuous topo-
graphical features. The highest land in the whole area is situated
near the north-west corner of the Temiscaming sheet, immediately to

* Bull. Geol. Soc. Am., vol. V., pp. ()20-(J26 with two maps, also American
Geologist, vol. XIV., Nov., 1894, pp. 282-285.
t Ihid, vcV XVIII, August, 1806, pp. 108-120.

22 I

NIFISSINO AND TEMI8CAMINO HEfllON.

the west of Lady Evelyn (Mus-ka-na-ning) Lake, where a range of hills
of which Maple Mountain is the highest peak, i-Ihch to tht; height of a
little over 2000 feet above the sea, according to Dr. Bell.

[nflutmcf of The influence exerted by the underlying rook on the general con-

iiiulo'i-lying . , 1.11 -1

rockonMuifucc tour ot tlio surface, is perhaps nowhere better exemphned tlian in the

contour. region embraced in this report. In the southern imd south-eastern

portions, where the prevailing rocks are the various gneisses and
granites included as Laurentian, there are no hills of any great height,
the general surface presenting, as usual, a rather monotonous succes-
sion of low rounded hills, with correspondingly shallow rocky valleys.
In the northern and wistnrn portions, however, tho.so arous in which
the ([uartzites iire present, as well as those in which the plutonic
rocks, chietly granite and diabase, are prevalent, rise into rather
important elevations ; while in those regions which are underlain by
the slaty member of the Huronian, are on the other hand low and flat.
A remarkable resemblance exi.sts between the contour of the surface,
occasioned by the presence of the diabasic rocks, and that jiroduced
by the heavy-bedded and massive quartzite, that forms the highest
member of the Huronian exposed in this district, both rising into
compatatnely high rounded or broken ridges, and rendering the
stretches of country where such rocks prevail, exceedingly rough and
hilly. This is especially the case with the region to the north and
north-west of Wakemika and Lady Evelyn lakes, and also between
Friday and Whitebear lakes and the Montreal River ; although the
whole of the area coloured on the map as underlain by those rocks
partakes essentially of this rugged character. This rough and broken
contour is in marked contrast to the flat surface cliaracteiistic of the
region in which the slates obtain.

The contrast is probably nowhere better shown than in the north-
eastern part of Lady Evelyn Lake, where the quartzite which crosses
the lake at the Obisaga Narrows forms high and perpendicular cliflFs
for a short distance, while to the east, as far as the Waswaning Nar-
rows, the shore on both sides is low and swampy, with only a
very occasional exposure of the flat-lying slaty rocks. At the elbow
to the east of the Waswaning Narrows, a high ridge of diabase crosses
the lake, forming rugged hills which constitute the western side of that
portion of the lake known as the Mattawapika. Thus within a few
miles, on the same lake, are exhibited examples of all three types of
surface produced by the underlying quartzite, slate and diabase.

Character of The large area coloured as granite, to the north-east of Lake Tema-
granite areas, gami, may perhaps be best described as a region of flooded roches

Examples of

differing

tojwgraijhy.

hollow
lakes o
and Ml
united
Pro!)
sented
the ()M
rooky
which
surface
indicate
sion, th
below t
lake, wl
gray un
before t
mouth o
vail, but
expansio
face of tl
usually
an asce
country i
hills are i
The M
Sturgeon
depressioi

The d is

known as

The Ottav

Mattawa i

panying n

the confin(

by far the

maps. Tli

3000 squa

square rail

Otter-tail i

smaller tha

of considei

included ir

(.A mow.

UENKKAL ITIYSICAK FEATUKKS.

23 I

inorutonnilea, for tlie hills art! ull low and rounded, while the interveninj;
hollows aro occupied by exceodinf,'ly intricate and shallow, swampy
lakes or marsheH. Tho valleys ot" the smaller rivers are usually narrow,
and many of the streams are nothing l)Ut a succession of small lakes
united by rapid rocky or bouldorv discharginf; clumnels.

Probably one of the most interesting of the physical features pre valley ,,f
sented by the district is the valley occupied by Lake Temiscaming and '"Vy.'V l^'^*^^"^
the Ottawa lliver. The greater portion of this valley is a very steep, TfiniKciuning.
rocky g<>rg", fringed on either side by lofty hills or perpendicular dill's
which rise abruptly to a height of from 100 to 000 feeot above the
surface of the water, while the average of a largn number of soundings
indicate that the lake has a mean depth of over 400 feet. The depres-
sion, therefore, occupied by these watei's would be about 1000 feet
below the level of the surrounding country, and as the bottom of the
lake, wherever examined, consisttsd in the deeper portions of a very line
gray unctuous clay or silt, this depth nniy have been much greater
before the accumulation of this material. I'^om Mattawa to the
mouth of the Moi u oal River, these abrupt and rocky shore-lines pre-
vail, but above the mouth of this stream the lake undergoes considerable
expansion and the shores exhibit a more gradual slope towards the sur-
face of the water. The traveller ascending the Ottawa lliver is thus
usually impressed with the mountainous character of the district, but Adjoining
an ascent of the hills on either side at once shows that the adjoining '^" ' ' ' '
country is comparatively level, and that what appeared as ranges of
hills are in reality the inclosing walls of this great valley.

The Mattawa and Montreal rivers and in a lesser degree the
Sturgeon and Ttmagami rivers occupy rather deep and ia\portant
depressions in this rocky plateau.

The district is traversed with rivers which are as important and well ]^.^\^^.^
known as the lakes which they .serve alternately as inlet and outlet.
The Ottawa is of course the largest, but only a portion of this, from
Mattawa to Lac des Quinze is included within the area of the accom-
panying map-sheets. The Sturgeon likewise finds its source beyond
the confines of this region, as also does the Montreal River, although
by far the greatest portion of both streams is represented on the present
maps. The Sturgeon is the larger of these two rivers, draining about
3000 square miles, while che Montreal drains an area of about 2500
square railes. The Matabitchouan, Mattawa, Keepawa, Temagami,
Otter-tail and Otter rivers are also worthy of mention, although much
smaller than the rivers first named. The Blanche River is a stream
of considerable size, but only a small part of the lower portion is
included in the Temiscaming sheet.

Kivcr vnlleys.

24 I

NIPISSINCJ AND TRMISCAMINCJ REGION.

Lakes. In coramon with other regions characterized by the presence • of

Archaean rocks, this district is remarkable for the number of
lakes both large and small which are scattered over its surface.
These lakes are in themselves noteworthy, not only for their many
intricacies, but also because of the great number of islands which

Distribution dot their surfaces. At first sight these lakes are seemingly governed

dependent on |jy j^q i^^^ jj^ regard to their distribution, but a somewhat closer exam-
geological •' ° ' . ,
structure. ination reveals the dependence of geographical outline on the geological

structure. In order to bring out more fully uhe intimate relation sub-
sisting between the topographical outline and the nature and attitude of
the enclosing strata, a careful compilation and correlation Oi^ the various
strikes or direction of the foliation of the j'neisses has been m-'de, exhibit-
ing with as close an approximation to the truth as is possible the various
curves and folds assumed by these rocks.

Principal "phe following nine lakes, with their areas and elevation above mean

sea-level may be particularly noted : —

Area. Height

Square Miles, above sea.

Lake Nipiasing 345 640-5 6478

" Temiscaming 125 577 S-Ogi-S

" Keepawa 120 87;V7-883

" Temagami. 100 964

Lac des Quinze 40 845

Lady Evelyn Lake 18 930

Obabica Lake 11 932

Obashing Lake 11 822

Rabbit Lake 8 938

Outlets of Lake Temagami, during the earlier portion of the summer, drains

Temaganii. both northward, by way of Nonwakaming and Lady Evelyn lakes

into the Montreal River, and southward by way of Cross Lake and

Temagami River into the Sturgeon, the water thus ultimately finding

its way into Georgian Bay and Lake Huron. The southern outlet,

however, is the larger and deeper stream, while the northern one is

>-v , . j, usually dry towards the end of July each summer, and is thus only

Rabbit Lake, utilized in time of high water. Rabbit Lake finds its main outlet

into the Matabitchouan River from the north-east corner of the

lake, but a bay extending to the south-east is connected at extreme

high water with Ross and Burwash lakes at the head of Macdonald

Creek, which in turn empties into the Matabitchouan River at the

Anninia- Fourth Bass Lako. Annima-nipissing Lake, a large and important

iiipissing sheet of water situated between Lake Temagami and the Montreal

Lake. . . ,

River, which has usually, as the name implies, been regarded as the

Elevations of ultimate source of the Nipissing water, is 1070 feet above the sea, while
highest lakes. Qpeeches Lake, which is in reality at the summit, is 1085 feet above the

•]

DENUDATION.

! i

sea. The highest lake in the whole region is Wilson Lake, at the
head of one of the branches of the Matabitchouan River, and this is
1173 feet above the sea, while the height-of-land between this lake and
the Montreal River is a little over 1200 feet above the sea

Dermdatlon.

In many of the descriptions which have from time to time Pre-glacial
appeared concerning this, in common with other Archwan regions, «'^'=''^'"tio"-
undue prominence has been given to the erosive effect produced dur-
ing the glacial epoch. The prodigious number of lakes both great and
small which are .so eminently characteristic of districts "r'^erlain by
Archwan rocks, have in general been referred to as original rock-basins
which owed their existence to the excavating power of an immense
glacier, while the maramillated hills and complementary valleys every-
where prevalent, as well as the constant occurrence of parallel
grooves and scratches, have been adduced as additional evidence of
the adequacy of the glacier to produce all the inequalities of the
existing surface. The detailed examination of the region, however,
amply demonstrates that the sculpturing to which the surface owes
its present configuration, was practically completed long before the
advent of the glacial epoch, and that the main valleys, especially those
of the Ottawa and Mattawa rivers, were in existence long prior to
the deposition of the Pala'ozoic sediments.

In the first place, the more important lakes and rivers occupy such Depth of the
deep and extended depressions that seem inexplicable on any theory ""^ ^" '"J**-
of glacial action or ordinary erosion by water. The bottom of Lake
Temiscaming 's on an average about a thousand feet below the level
of the surrounding country, and in no place did the sounding lead
reveal the original rocky bbttora which has been more or less deeply
covered by silts and by accumulations of drift material. Portions of
the Mattawa and Mon'^ieal rivers are fully six hundred feet below the
level of the roi ky plateau through which they flow, and in many places
exhibit steep, often peipendioular banks, composed of the hardest and
most massive crystalline rocks,

Secondly, the trend of many of these valleys 'oes not coincide with Many valleya

the general direction of the ice-flow, as revealed by the stria' and "'?t odincKlent
f _ T J \\\t\\ direction

grooves which mark many of the exposed rock-surfaces of the plateau, of ice flow.
These striae in general vary from S. 10° W. to S. 30° W.,
while S. 20° W. may be assumed as a fair average of the direction
of the ice-flow throughout this region. The deepest valle}', that occupied

■ i^i\

! I

26 I

NIPISSIKG AND TEMISCAMING REGION.

■ARLOW,

Some sti'iiu
coiTospond
with direc-
tion of certa
valleys.

Valleys not
corresponding
wit!) strike.

Cut in rocks
of different
composition.

Valley of
Montreal
River.

by liake Temiscaming and the Ottawa River, from the mouth of Wabi
Creek to its confluence with the Mactawa River, has a direction of S.
30° E. while the valley of the Mattawa runs about east-and-west, thus
forming consideraljle angles with the general striation, while the Mon-
treal and Sturgeon rivers are intersected almost at right angles by these
grooves and scratche.s. On the shores of Lake Temiscaming, and also
on the JNIontreal River, many of the stria? exhibited have a direction
corresponding with these valleys. These may either represent a dif-
ferential iMOveiuent in the mass of the ice itself, whereby the lower
portion was forced by reason of its plasticity, to conform to the
inequalities of the existing surface while the upper portion continued
on its general south-wesierly course ; or, as seems more probable, these
grooves may have belonged to a local glacier occupying these valleys
towards tiie close of the glacial period. On the upper or wider portion
of Lake Temiscaming, stria> belonging to the general glaciation may
be noticed on the same rock-surface as other markings which belong
to this local glacier, but the more abundant and strongly marked
grooves throughout the lower portion of the valley, are seen conforming
to its various changes of direction.

Again, many of these valleys do not correspond with the strike of
the rock in their immediate vicinity. The Ottawa valley is the best
illustration of this fact, for the foliation of the gneissic rooks which
compose most of its shores intersect tliis gorge almost at right angles.
The depressions occupied by tlie Sturgeon and Montreal rivers also
form considerable angles with the strike of the rocks in the immediate
neighbourhood. Very often the streams occupy singularly straight
and deep chasms in very hard rocks of different composition, valleys
which it seems impossible that the ordinary erosive action of ice or
water could ever have opened up, and which preserve their uniform
direction with very little deviation in their course even when the river
has left a softer rock to enter an area where the hardest varieties
prevail.

The Montreal River, from "The Notch," near its mouth, to the
bend above the portage to Mud Lake, a distance of twenty-one miles,
flows through a rocky gorge, the course of which is in general N. 40°
W. At this point the course of the valley changes abruptly to S.
45" W., which is maintained till Bay Lake is reached, a distance
of four miles. From this point upw.ird a valley extends as far as
the (Jreat Bend, beyond the confines of the present mtp, which is
almost if not quite parallel to that occupied by the river below Mud
Lake portage. Of course the river presents many minor deviations in

its dow
the vulj
success]
characti
little or

The e

these va

early tii

conglora

Logan c

shallow I

the Hun

senting t

fringe fn

Temiacac

west side

stones ari

the penin

limits of

the eastei

angular o

which foi

These det

talus, fori

ence took

composed

with a sm

grit rest uj

before tlu

glacier flo\

polished tl

the meshes

hillocks.

resting on t

six miles

Rivieres, a

sandstones

no fossils, \

The occu
valleys she
indicate the

■ARLOW,

]

DENUDATION.

27 I

its downward course, but the remarkable uniformity in direction of
the valley through which the stream meanders, ia maintained through
successive alternations of slate, quartzite, graywacke and diabase, the
character and composition of the surrounding rocks having apparently
little or no effect in determining the course of this depression.

The existence, likewise, of Pahi'ozoic outliers occupying portions of Paheozoic
these valleys, seems ample proof of their existence as such from a very "" "''^^'
early time. The occurrence of an outlier of limestones, shales and
conglomerates belonging to the Niagara, was noticed by Sir William
Logan on Lake Temiscaming in 1844. This outlier appears as a
shallow syncline resting unconformably on the slates and quartzites of
the Huronian. The conglomerate, grit and arenaceous limestones repre-
senting the basal portion of the section, may be seen forming a narrow
fringe from Piche's Point to Chiefs Island, on the east side of Lake
Temiscaming, while a small patch of similar rocks crops out on the
west side from Haileybury noitliward towards Wabi Bay. The lime-
stones ai-e present on the islands to the north of Bryson Island, and on
the peninsula between Suttons and Wabi bays extending beyond the
limits of the present map. The boulder-conglomerate that occupies
the eastern shore to the south of Chiefs Island, is composed of large
angular or subangular blocks derived from the Huronian quartzite
which forms rather abrupt hills immediately behind this exposure.
The.se detached fragments doubtless repre.sent what was originally a I ',;(«»! bwls of
talus, formed at the foot of this steep slope, and when the submerg- * '"■!?"■"»•
ence took place, the intervening spaces be;.- :. ^'.lA v, detritus
composed of the same materials, in a finer iilatt i iS together

with a small proportion of calcareous matter, ' His- con,^ "ate and

grit rest upon a surface which had clearly ass lju) J a hammock} character
before the depo.sition of these sediment? • 'he acf/ion of the

glacier flowing down Lake Temiscaming 1 - ■ *•* • ' „..iated and
polished the whole, leavir.ga surface with a net-like struttui'e, through
the meshes of which protrude rounded or ovoid sections of these rocky
hillocks. Limestones and sandstones of Black River age are seen FUiKk River
resting on the mammillated surfaces of Laurentian gneiss on the Ottawa, '""^* ""^'
six miles below Matttwa, and also about five miles above Dei'x
Rivieres, as well as on the Manitou Islands, Lake Nipissing, while
sandstones which are probably of Chazy age, but which have yielded
no fossils, were noticed on Iron Island in the same lake.

The occurrence of such outliers at various points throughout th^se Tiansgienaion
valleys show that they existed in very early Paheozoic times, and "^ Pivlseozoic
indicate the transgression of the sea thus far inland at intervals during

\lv

28 I

NIPISSING AND TEMISCAMING REGION.

M ;',

numincjckf.

Pre-glacial

rock-surface.

Cliffs along
lakes and
rivers.

this, the Paheozoic, \ he submergence having been greatest during the
Niagara, when the sua reached the northern end of Lake Temiscaming
and may possibly have been connected by narrow arms and straits
with that extending southward from Hudson Bay.

The rounded or moufonn^e surfaces of all these rocky elevations,
though no doubt accentuated by later glacial action, have in the first
place been due to the unequal progress of rock decay. The work of
Lawson, Low, Coste and Laflamme,* who have during the progress of
their several explorations made critical and extended examinations of
the relations existing between many outliers of Palaeozoic strata and the
subjacent Archtean rocks, clearly shows that the mammillated surface
long antedates the glacial epoch, and was as characteristic of the surface
upon which the earliest Palaeozoic sediments were deposited, as that
upon which the great glacier rested in glacial times. The chief
cavities, vertical precipices and deep, narrow gorges must have been
determini'd by great transverse or lateral breaks. The causes which
operated in their formation must have been in force with marked
intensity long before the deposition of the Niagara, for as has been
shown, the valley had been practically completed before the depc :-
tion of these sediments. The rounded contours of the rocky plateau
and the intervening hollows, doubtless represent the depth to which
these crystalline rocks had undergone disintegration during the
immense la[)se of time while they were exposed to the action of the
weather and other denuding agencies before the glacial epoch, while
the ice simply removed the loose material resulting from such decom*
position, smoothing and striating the rocky surfaces encountered.

Both quartzite and diabase, and sometimes also the massive slate
(or graywacke) which occurs as a transition between the more fissile
slate beneath and the quartzite above, frequently from cliff's
from fifty to two hundred feet in height, the angle of slope
being considerably lessened by a talus of angular blocks detached
from above. Goiid examples of these quartzite cliffs are furnished by
the shores on the west side of Lake Temiscaming, opposite Bryson
or Moose Island, at th(3 Obisaga Narrows on Lady Evelyn Lake, as
well as by the steep hills on the west side of Cliff" Lake, while the
Manitou or Devils Rock on the west side of Lake Temiscaming, south
of Haih>ybury and the western shore of Temagami Lake, opposite the
Hudson's Bay post are excellent instances of the vortical precipices
produced by exposures of diabasic rocks. Prominent cliffs formed of

* Bull. (Jeol. Moc, Am., vol. T, pp. 1(53-173, also Annual Ke|xirt, Geol. Surv.
Can., 1882-83-84, part n.

BARLOW 1

the ma!
Kiver ii
of Lad;
frost an
which t
that one
garni, hf
the caua

Althoi
agricultu
land are
are to be
earning oi
although
Lands De
Gluigues a
Baby and
this side,
On the op
into lots, t
of the lak
valleys of
five of the
eluded wit

The area

rolling cla\

loam or sai

appears at

has in man;

fire.s, this c

Quinn Poi]

gray clay th

of quartzitf

rise abrupt

characterize

appearance

On the t
and broken.
Along the

»OIL.

29 I

the massive slate or graywacke may be noticed on the Matabitchouan
River immediately above the Fourth Bass Lake, as also on the west shore
of Lady Evelyn Lake, south of Wendabin Bay. The action of the
frost and weather are continually loosening large masses of these cliffs,
which then fall witii a great noise, and this phenomenon is so fie(juent
that one of the lakes (iNIanito-peepagee), to the west of Lake Tema-
gami, has received its name on the supposition that the Evil One was
the cause of the disturbance.

SoU.

Although the district as a whole cannot be said to be suitable for Areas of
agricultural purposes, still in many places considerable areas of good '""'"
land are known to exist. The largest continuous tracts of such land
are to be found in the vicinity of the northern portion of Lake Temis-
caming on both sides of the lake, and thus both in Quebec and Ontario,
although the larger proportion is in the latter province. The Crown
Lands Department of Quebec has sub divided the two townships of In Quebec.
Guigues and Duhamel and portions of four others, Fabre, Laverlochere,
Baby and Neudlac. These by no means exhaust the arable land on
this side, but are sufficient for the present requirements of settlement.
On the opposite shore of the lake, Ontario has laid out and divided In Ontario.
into lots, twentj'^-five townships which extend along the western side
of the lake, and running in a north-westerly direction include the
valleys of Wabi Creek and the Blanche as far as Round Lake. Only
five of these townships and the southern portion of four others are in-
cluded within the "v ja covered by the accompanying map.

The area thus sub-divided is in general composed of level or slightly Cliarauter c.f
rolling clay land. In some places the clay sub-soil is overlain by clay
loam or sandy loam, while in other instances a rather barren yellow sand
appears at the surface. In the province of Quebec, where the surface
has in many places been almost completely denuded by repeated forest
fires, this clay is best seen. From the Quinze River a little south of
Quinn Point, large areas are covered with a thick mantle of stiff (;>i,^y .,i_.ji„j,
gray clay through which protrude exceedingly rough and prominent hills
of quartzite, granite, diabase and breccia-coni.'lomerate. These hills
rise abruptly from an otherwise level clay plain, for the surface
characterized by the presence of this clay exhibits a singularly flat
appearance with only a gentle rise towards the base of the hills.

On the Ontario side, the township of Lorrain is rough, rocky Lwriin.
and broken, and for the most part unsuitable for farming purposes.
Along the valleys and in the vicinity of Lake Temiscaming the soil

30 I

NIPIS8ING AND TEMI8CAMINO REr.ION.

Bucke and
Dyuioud.

Linu'stone
plateau.

Hiuhun and
Henwiiod.

Valley of
Mattawa.

Valley of
Sturgeon
River.

Kinoky I''m11s
and Teuiagumi
Kiver.

is clay, but these clay flats are of comparatively small extent. To the
north-west, however, in the townships of Bucke and Dyraond there are
quite a number of farms, and a large area of cultivable land exists, so
that the villages of Haileybury and Liskeard seem destined to become
the centres of a considerable agricultural community.

The top of the limestone plateau which constitutes that portion of
the Niagara outlier forming the promontory dividing the northern end
of the lakp, is generally overlain by a light sandy loam soil, although in
many places the underlying rock is destitute of any such covering. • In
the south-western part of Dymond and the southern portions of
Hudson and Henwood, a series of rocky ridges of the Huronian slate
occur. In the township of Henwood these ridges have a general north-
and-south trend ; while in the township of Hudson the slate rises into
hills some of which are nearly 200 feet in height. North of these
ridges, according to Mr. Hermon, the soil is white clay, the surface
generally level and the appearance of the couutiy flat and swampy.

Between Mattawa and North Bay, to the south of the Mattawa
River, in the townships of Papineau, Calvin, Bonfield and Ferris, con-
siderable areas of l.'ind exist which may be utilized for farming pur-
poses, and their proximity to the line of railway makes these of value.
Already these townships contain a large number of excellent farms
and the region is rapidly becoming settled. The soil is usually a clay-
loam, rather rocky and stony in places, but seems to yield excellent
crops. In the vicinity of North Bay the land is sandy and light.

The valley of the Sturgeon, below the Temagami River, contains
many wide and extensive flats which are susceptible of improvement,
but above this stream the valley is much contracted and the flats
decrease both in number and extent as the river is ascended, and
towards the mouth of the Maskinonge River the country becomes much
more broken and for the most part poor and rocky. Between Smoky
Falls and the mouth of the Temagami, the country in the vicinity of
the river is tolerably level and composed of gray clay overlain by sand.
The soil is for the most part a sandy loam and affords support to a thick
growth of hardwood and evergreens which by their sturdincss attest
the good qualities of the soil beneath. Clearances have been made at
intervals along the river, with the exception of that portion flowing
through the Indian reserve, as far as the mouth of the Temagami, A
short distance below the mouth of the Pike River, on the south side of
the river, is an axtensive farm cultivated for many years for the pur-
poses of supplying the lumbering camps of Mr. J. R. Booth, and a
roii'J connects this depot with the Canadian Pacific Railway at Cache
Bay station.

CLIMATE.

31 1

To the west of Sturgeon Falls there are a large number of farms W-uve River,
which continue up the valley of the Veuve River, almost as t'ar as
Warren station, where the valley becomes very narrow. The soil
throughout the valley is a stiff gray clay, and as the vegetable mould
overlying has been burnt off it has a tendency to cake in dry weather.
In the vicinity of Sturgeon Falls the soil is very sandy, but the clear- Near Sturgeon
ances continue to the east as far as the boundary of the Indian
reserve, and to the south almost to the lake shore, although the land
in general in this direction is flooded during the spring freshets.

On the Montreal River above Bay Lake, there are large areas of Montreal
arable land, especially between Bay Lake and the Mattawapika. The
region to the north-west is very flat and level, underlain by clay^
and althoujih swampy at present, would probably be easily drained or
dry up when cleared. These areas are most likely continuous with
similar tracts noticed to the south-west of the townships of Henwood
and Hudson.

A large tract of country extends from the vicinity of North Bay lietweeii
and the southern part of the townships of Widdifield northward to (n,,! (),,i,„'ii;a
the Opimika Creek. The soil is in places sandy and in some spots I^*'"'"^^'*'
considerable clay is present, but the whole of this stretch of country
is covered by a mixture of hardwoods and evergreens, thus denoting
a rather good soil beneath. The greater portion of the district, how-
ever, is extremely rocky and barren, the level areas being chiefly occu-
pied by swamps, many of which would be ditticult to drain, while the
area thus drained would in most cases be insufficient for purposes of
farming. Of the country surrounding Temagami Lake and the greater Oreat \»Tt of
part of the central portion of the area, only small tracts would be al)le for
available for purposes of settlement. The soil in general is extremely ^'^''"''"K-
light and without the aid of artificial fertilizers would soon fail to
yield any adequate return. The rosy picture too often drawn of
immense tracts of land available for agricultuial purposes, is to say
the least very misleading, for apart from possible mining and its timber
resources, by far the greater portion of the region will only be valuable
as a health and recreation ground for tourists and sportsmen The
great tracts of forest as yet untouched by the axe, the vast number of
picturesque lakes, both great and small, with fish and game in abun-
dance seem to render the district especially attractive for such purposes.

Climate.

In regard to the climate of the district as a whole, it may be said (Jcneral
in a general way, that the advent of spring is from three weeks to a [;|™aeter

32 I

NIPISSING AND TEMISCAMING REGION.

Oijeniiig of
navigation.

Closinfc.

Progi'f'ss I if
spring.

'■: I ;

Harvest.

Summer
frosts.

month behind that of the region immediately surrounding the city of
Ottawa, with a correspondingly earlier setting in of the winter. The
winter is as a rule one of long continued and severe frosts, while the
summer is proportionately shorter and much cooler than the country
bordering the lower Ottawa. The average fall of snow in winter as
well us th(! rainfall during summer is likewise considerably in excess of
that in regions further to the south.

Navigation generally opens on Lake Temiscaming about the end of
the first week in May, although in occasional unfavourable seasons it
is sometimes delayed a few days longer, while Keepawa Lake does not
usually break up till a week later, In 1893, the ice on the latter lake
broke up and moved out between the 15th and 17th of May. Lake
Temagami, which occupies the heigh t-of-1 and between the waters flow-
ing to Lake Temiscaming and those emptying into Georgian Bay, being
nearly 400 feet above tlie last-named lake, does not generally break up
till the latter part of May, the lake usually being clear of ice about
the 24th of May. The season of navigation closes, as far as Lake
Temagami is concerned, between the 10th and 15th of November,
while on Lake Temiscaming steamers have been known to make fairly
regular trips within a few days of Christmas, although as a rule these
boats cease running early in December.

The snow begins to melt about the middle of A.pril, and has gener-
ally all disappeared by the 10th of May, although both snow and ice
were noticed in secluded nooks and cracks along the sides of the
precipitous cliff's on the west side of the Ottawa River as late as the
end of May. Mr. C. C. Farr, formerly of the Hudson's Bay Company,
and now postmaster of Haileybury, who has become identified with
this young and flourishing settlement, states that " seeding-time com-
mences about the first week in May and ends, so far as oats are con-
cerned, about the fourth of June, though oats have been sown as late
as the 20th of June, and have done fairly well. Potatoes can be
planted as late as the 20th of June, and it does not profit much to
put them in before the 24th of May. Corn, cucumbers and melons
can be sown about that date. Haying commences about the 14th
July, harvest the loth August."

Summer frosts, so much dreaded by the farmers, specially in districts
newly opened for settlement, have in the past proved a rather serious
barrier to the successful raising of wheat, while oats have suflFered
severely, particularly in clearances situated some distance from the
larger bodies of water. Frosts generally occur from the 18th to the
25th of August on the calm, clear nights following heavy north winds.

TIMBER.

33 I

In the vicinity of Lake Temiscaining the settlers often escape
them altogether on account of their proximity to this large sheet of
water, or their crops are but slightly injured, the more tender vege-
tables frequently being the only sufferers. The gradual clearing up of
the land and the draining of many of the swamps will, however,
materially mitigate this difficulty, particularly in the district in the
vicinity of Lake Temiscaming, which is the area most suitable for
extensive settlement.

The Native Inhabitants.

The Inflians who reside within the area under description belong to imlians.
the once numerous and powerful Algonquin family. They speak the
Otchipew or Chippewa language, the same as that in use among the
many bands which are scattered over the wide territory to the north
and west of Lake Superior, with only a few minor alterations. They
are divided into three bands known respectively as the Nipissing,
Temiscamingue and Temagamingue bands. On June 30th, 1887, the m. • , .
census taken by the Department of Indian Affairs showed a total
Indian population of 394, while on June 30th, 1897, this population
had only been increased to 430. The census taken in 1887 showed
the following numbers in each band, Nipissing 165 Temiscamingue
136, and Temagamingue 93, while that taken in 1897 shows the popu-
lation of the several bands to be, Nipissing 193, Temiscamingue 162,
and Temagamingue 75. While therefore the total Indian population
of the district shows a slight increase, one of the bands (Temagamingue)
is slowly but surely decreasing. Two of the bands are comfortably
settled on spacious reserves but no tract of land has yet been allotted residence.
to the Temagamingue band. The Nipissing band resides chiefly in two
small villages situated on the north shore of Lake Nipissing. The
larger of these is about two miles west of North Bay to the south-
west of Beaucage station on the Canadian Pacific railway, while the
smaller one is located near the western boundary of the reserve, about
four miles south east of Sturgeon Falls. The Indians and associated
half-breeds have built a considerable number of rather substantial
dwellings, each with a small cultivated patch attached, on the northern
bank of the Quinze River, forming the village or settlement of North
Temiscaming.

1 Mi
I

Timber.

All the early explorers speak in terms of enthusiasm of the original White pine,
great forests of the region here described. The most valuable tree from
3

34 I

NlPISSmo AND TEMI8CAMING REGION.

•kHUlW

I' I

a commercial standpoint is the white pine (Pinus Strobus), and in
spite of tl»e extensive operations carried on almost uninterruptedly by
the lumbermen throughout a large part of this region during the past
fifty years, this tree is still present in considerable quantity. Next
Red pine. in importance and more abundantly distributed is the Norway or red
pine (I'inus reshiosa.) In the early years of the lumber trade, the
greater value of this tree caused it to be sought for at more remote
distances than the white pine, and thus we find at this time that
camps for cutting red pine timber were many miles in advance of those
erected for the purpose of securing white pine loi^s. The superior
qualities of the white pine, however, soon came to be recognized and
in time completely drove the red pine from the market, or so limited
its sale that only a few of the finest trees were hewed down and
utilized. Of late years, however, the marked diminution in size and
quantity of the white pine has again brought the red pine forward, and
both varieties are now cut without discrimination. The red pine seems
to flouiish on the apparently sterile sand plains, which are a feature
in many parts of this district, and frequently forms excee('ingly thick
groves on the sides of hills where sand and gravel have collected, or
on points composed of these drift materials which jut out into many
of the lakes.

Jack-i)ine. Jack-pinc, called by some, pitch-pine, or bastard spruce {Pinus

Banksiana) is very often encountered in the more barren and rocky
areas, and its presence seems an almost certain indication of the ex-
treme poverty of the underlying soil. It is usually more or less
scrubby or stunted in its growth, although occasionally, as in .some
areas to the north-west of Lake Temiscaming, it attains sufficient dim-
ensions to be utilized for rough lumber. In the vicinity of the south-
ern and eastern shores of Lake Nipissing, the scanty groves of dwarf-like
evergreens are almost wholly composed of this species, the hardy roots
penetrating the various cracks and crevices of the rock. This tree
S'lso seems to select sandy or gravelly plains which have been overrun
by fire and which had previously been occupied by a luxuriant growth
of red or white pine.

Spruce. Both white and black spruce (Picea alba and Picea nigra) are fre-

quently met with, the latter being more abundant, but are too small
to be of any commercial value for lumber, although many individuals
would make excellent masts or spars.

Cedar. White cedar (Thuya occidentalis) is usually found fringing the

banks of streams or the shores of lakes, where it often forms a thick
and at times an almost impenetrable undergrowth. Overhanging trees

are free
high wj
©red, b<
marshy
hills, an
a dense
less stur
hollow a
many tin

The w

occurren

second gi

species in

though s

green, esj

large tree

as in the I

be procure

Temagami

of their ki

of good an

Three vj

the balsam

or aspen p

Of aspen (

stately tree

country to

arac, someti

A mericana)

degree the s

forest where

immense tra

iko and Otte

abundant su

stantly met '

favourable tc

The balsan
the moist ai
ward to the I
below the a
observed as ;

TIMUEK.

are frequently undermined by the waters or current during tikiies of
high water, and thus it happens that most of the drift-wood encount-
ered, belongs to this species. Its favourite haunt also seems to be the
marshy hollows or tlats, which so commonly occur between the rocky
hills, and extensive areas of swamps are almost entirely covered with
3. dense forest (jf this tree. As a rule, the tree is small and more or
less stunted in its growth, while the larger individuals are frequently
hollow at the butt. To the north and north-west of Lake Temiscaming
many tine specimens of this tree were noticed.

The white or canoe birch {Betufa papyri/era) is also of very common W)\ite liirch,
occurrence, and together with the aspen poplar forms the prevailing
second growth in areas which have been recently swept by fire. Both
species in these instances form very thick groves of tall and straight
though small trees. Interspersed with the more prevalent ever-
green, especially where the soil is deeper and better, are occasional
large trees which are of sufficient size to furnish good bark for canoes,
as in the Sturgeon River valley, where good sized specimens may still
be procured. The birch-bark canoes made on Lakes Nipissing and
Temagami and at Mattawa, have always been considered the very best
of their kind both in build and material, but of late years the supply
of good and suitable bark is becoming perceptibly less.

Three varieties of the poplar were noticed throughout the region Poijlar.
the balsam or rough-barked poplar {Populus balsamifera), the white
or aspen poplar (Populus trernuloides) and the large toothed poplar
or aspen {Populus grandidentata). The poplar sometimes forms
stately trees, especially in the Sturgeon River valley and in the
country to the north and north-west of Lake Temiscaming. Tarn- Tuiniirac.
arac, sometimes called hackmatack and occasionally juniper (Larix
Americana) is abundant, and in common with the cedar and in a lesser
degree the spruce, affects the low-lying areas or those portions of the
forest where moisture nay be readily and constantly secured. The
immense tracts of swampy land between the head-waters of the Tom-
iko and Ottertail rivers to the north of the Spruce Lakes contain an
abundant supply of good sized specimens of this tree, and it is con-
stantly met with all through the region whenever the conditions are
favourable to its growth.

The balsam or fir {Abies bahamea) is one of the most common in BmIsuh..
the moist areas. Hemlock {Tsuga Canadensis) was noticed north- H.mlDLk.
ward to the Indian portage-route to Keepawa Lake, a short distance
below the mouth of the Keepawa River, but no specimens were
observed as far north as the Old Fort Narrows. It occurs rather

36 I

NIPISSINfJ AND TEMISCAMIN*; REfilON.

•ARLOW.

il
i

I I

i I

r>aHH\V(K)(l.

Yew.

Al<]er and
willow.

abundantly and of large .size in the vicinity of Lake Nipissing and on
the Sturgeon River, but was not remarked in the northern and north-
western portions of the region. The basswood or linden tree ( Tilia
Americana) was occasionally noticed on the Sturgeon River, while Sir
William Logan mentions individuals two feet in diameter, associated
with black birch and maple of similar dimensions, in the hardwood
strip of country extending from behind the hills north of Trout Lake
at the head of the Mattawa River to the Opimika Narrows on Lake
Temiscaming. The basswood was also noticed mixed with maple, elm,
poplar and balsam near the mouth of the Blanche at the north end of
Lake Temiscaming.

The American yew, sometimes called ground hemlock {Taxus haccata
var. Canadensis) is an exceedingly common shrub, and is particularly
noticeable, as when present it often forms an almost impenetrable un-
derbrush. Alder and willow of several varieties are present in the
various swamps or lining the banks or shores of streams and lakes.

scarce,
Maplp

Hardwood Although nearly all the principal varieties of hardwood are found in

a"ir.l. ' this region, the proportion which such trees bear to timber of a softer

description is quite insignificant. Of the maple family, perhaps the
most abundant is the sugar maple (Acer Saccharum), which is fre-
quently of large dimensions. The soft maple {Acer rubrion) is also
present in large quantities, but the black or bird's eye maple (Acer
nigrum.) is only rarely met with in the valleys of the southern portion
of the region. The mountain maple (Acer spicatuni) is one of the com-
mon varieties in moist ground, while the striped maple (Ao'r Pennsyl-
vanicum) was noticed in many places. This tree is often called
Moosewood, because the green and juicy tops form a favourite food for
the moose, although the true " moosewood " (Dirca palustris) was
noticed in many places suitable to its growth.

Moosewood.

Yellow birch.

lilack birch.

Oak.

Large trees of yellow birch (Beiula Intea) were remarked through-
out the region, especially in the vicinity of the northern end of Lake
Temiscaming, while specimens of the black or cherry birch {Betula
lenta) were seen over thirty inches in diamatfr in the region to the
north of the Mattawa River. The blue oak or swamp white oak
(Quercus macrocarpa) is the most abunda>;l 'A the oak family, and its
favourite haunt seems to be the alluvial flats or intervals along the
banks of streams where the soil is sufficiently moist and fertile. Here
it is associated with the white elm (JJlmus Americana), which forms
large and beautiful trees, the black or water ash (Fraxinus sambucifolia).
The white oak (Quercus alba) seems to delight in lighter and drier
soil, and good specimens were seen growing in the vicinity of Fort

Temiscaming. The
as far north as o
Virginica) is toleral
growing with the Ai
hardwood land abou
Temiscaming.

Of the wild fruits,

sparingly representee

trict on the Ottawa,

dant on all neglect

and in the vicinity oi

riparia) was seen gn

well as on several islt

low-bush cranberry ((

on many of the marsh

The former species is

swampy flats in the vi

Lake Nipissing is tl

formerly were a source

band of Indians, who

to sell to the traders o

variety of cranberry ((

command a sufficient j

The high bush cranb

along the river-valleys

low. Tiie bushes are

height, and are especia!

head of Lake Temiscamii

earning, and fringing t:

further to the south. Th

( Vaccinium Canadense a

which have been lately

known to set fire to som(

of this fruit. Vacciniun

locality, but is also freqi

posed to the sun's rays, v

ant though much better j

soil as well as localities v

Of the deer tribe the m
and the red or Virginia .

i v.i

•AKLOW. I

FAUVA.

17 I

Temiscaniing. The red oak (Quercus rxibra) was also noticed in places

as far north as our explorations extended. Ironwoo<i {Ostrya Ironwood.

Virginica) is tolerably abundant and good. Specimens were noticed

growing with the American beech {Fagu8 ferruyinea) in the strip of Bffcli.

hardwood land about five miles west of the Opimika Narrows on Lake

Temiscaming.

Of the wild fruits, the thimble berry {Rubua viUosua) is only very Berries,
sparingly represented if at all in the south-eastern portion of the dis-
trict on the Ottawa, but the red raspberry (Rubua slrigosus) is abun-
dant on all neglected clearingy, or in areas which have been burnt
and in the vicinity of deserted lumber camps. The wild grape ( Vitis
riparia) was seen growing on Mann Island, Lake Temiscaming, as
well as on several islands of Lake Nipissing. Both varieties of the
low-bush cranberry {Oocycoccus viacrocarpus and 0. vulgaria) are found
on many of the marshes which are so prevalent around Lake Nipissing.
The former species is the variety generally collected, and the extensive
swampy flats in the vicinity of the mouth of the Sturgeon River on
Lake Nipissing is the principal locality for these berries. They
formerly were a source of considerable revenue to the thrifty Nipissing
band of Indians, who took them in ban vis down to the French River
to sell to the traders on Lake Huron. Several barrels of the smalle**
variety of cranberry {0. vulgaris) were sent to Toronto, but did not
command a sufficient price even to pay expenses.

The high bush cranberry ( Viburnum Opulua) grows in damp ground
along the river-valleys or on the margins of lakes where the shores are
low. The bushes are sometimes between ten and twenty feet in
[height, and are especially abundant on the Devil's Channel, at th^
head of Lake Temiscaming, on the shores of Mann's Island in LakeTemis-
Icaming, and fringing the banks of the Little and Ottertail rivers
[further to the south. The two varieties of blueberry commonly met with
Vaccinium Canadense and V. corymbosum) are present on all surfaces
^hich have been lately swept by fir'^, and the Indians have been
:nown to set fire to somft of the smaller islands in order to get a supply
}f this fruit. Vaccinium Caiiadense prefers the drier and more rocky
locality, but is also frequently noticed in swampy flats directly ex-
posed to the sun's rays, while Vaccinium corymbosum with less abund-
Lnt though much better and larger fruit, prefers a deeper and richer
loil as well as localities which are more in the shade.

i'H

Fauna.

Of the deer tribe the most abundant are the moose (Alee <tmericanus) ^iq^.^^ ^nd
lid the red or Virginia deer (virginiamis Cariacus). Owing to the ''^^r.

i***

38 I

NIPI88ING AND TEMISCAMINQ REGION.

j'!

i\'

I, J!.'

Wolf,

Moose and
(leer moving
northward.

Caribou.

Fur-bearing
animals.

Small
iinima's.

recen*. provisions iiade by the Ontario Government looking to their
preservation, aided no doubt by the advance of settlement to the south,
these animals have become exceedingly numerous. The moose in par-
ticular is abundant, and their " runways " especially in the vicinity of
rivers and lakes off the frequented routes of travel, are usually better
beaten than many of the cattle paths in the neighbourhood of con-
siderable settlements. This is notably the case on the Ottertail River,
which (lows into Lake Temiscaming from the west about four miles
ajaove the Opimika Narrows, on the small stream connecting Boice and
Wicksteed Lakes as well as on the lower part of the Montreal River.
It is only within the last ten years that the red or jumping deer have
become at all numerous, and before 1887, only occasional specimens
were shot, but now every sandy beach in the more secluded portions of
the region is covered with the imprints of the feet of these animals.

The wolf (Canis lupus) has likewise become rather common, although
a few years ago tliey were rarely if ever encountered. These animals
follow very closely the migrations of the deei'.

Both moose and red deer are gradually moving northward and
north-westward, the former being met with in the vicinity of Abitibi
Lake where previously they were unknown, while occasional specimens
have been shot, according to Mr. A. P. Low, close to Moose Factory
on James Bay.

The woodland caribou (Ravgifer caribou) is not at all abundant,
and chiefly inhabits the region to the north and north-east of Keepawa
Lake, becoming more numerous to the noith east. The black bear
(Ursits americanus) is still a rather common animal, but the constant
demand for and ready sale uf the skins has led to their diminution.

Specimens of the fox ( Vrdjies vulgaris) are encountered and the skins
find a ready sale. The Canada lynx or wild cat (Lynx canadensis) is
likewise found, but only occasionally. The otter (Lutra canadensis)
and the beaver {Castor jibfr) are fast becoming extinct in this region,
although signs of their presence may still be seen on many of the less
frequented streams and ponds.

The tisher {Mustela. pennantii), the sable or marten {Miistela
americana), the stoat or ermine {Futorius ermineus), the mink {Pntorins
vison) and the muskrat (Fiber zibethicus) are also met with, and the
two last named are still abundant in the region. The skunk (Mephitis
mephitica) is very common, especially in the vicinity of the settlements
or lumber camps, where they come to feed on the rubbish thrown from
the kitchen.

The porcupine (Erethizon dorsatns), ground hog (Arctoinys monax)
and the hare or rabbit (Lepus anfiericanus) are also common.

The
noticed,
white pin

The hd
the most
is usually
titute of

The ra\
sible ledm
cip'v lotci!
the Roche
side of La

'■m

FAUNA.

39 I

Ducks com-

liarativfly

Kcarce.

Black and
wt)od duck.

The chipmunk or striped squirrel (Tamias sfriatus), the red squirrel or Stiuirni and
chickaree (Sciurus hudsonius) and the flying squirrel (Sciurapterus 'pn""' '•
voluceila) are likewise common throughout the district.

No special attention was devoted to noting the presence or habits of Birds.
the birds of the district, but a few observations regarding the most
noticeable ones may be of interest. Ducks are as a rule comparatively
scarce throi'ghout the greater part of the area, chiefly because of the
marked absence of wild rice, their favourite food, and the somewhat
rare occurrence of open marshes, their customary habitats. There are,
however, several very notable exceptions to this rule, and the shallow
swampy bays which characterize the west portion of Lake Nipissing,
the north-eastern extremity of Shabosagi or Wicksteed Lake, as well
as the northern end of Lake Temiscaming are favourite resorts for a
rather large number of ducks during certain months both in the
spring and autumn. During the summer months it sometimes hap-
pens in passing over the less frecjuented routes that occasional
specimens of the black duck {Anas obscura) and the wood duck [Aix
sponsc) are met with.

The merganser or saw-bill {Merganser americanns) isp. veiy familiar Merganser,
sight along the numerous waterways, especially at the foot of small
rapids.

Occasional specimens of the pied-billed grebe or dabchick {Podilym- H^ll-diver.
bus podiceps) were also met with. The great northern diver or loon
{Urlnator iniber) is also a common inhabitant of the district. With
few exceptions each of the small lakes has a pair of t-Ui^e birds, while
in the larger expanse.s of water every individual bay or arm contains
two loons, who year after year return with great regularity to Le
same locality for breeding purposes.

The osprey {Pandion haluLelus carolinensis) was frequently rish-hawk.
noticed, the nest being usually situated on the very summit of ji 'ofty
white pine " rampike."

The herrirg gull {Larus arffcntatus smithsonianus) is also one of Gull,
the most abundant birds of the lakes of this region. Its nestmg place
is usually on bare rounded hummocks of rock, almost completely des-
titute of soil or vegetation.

The raven {Corvus corax principalis) very often builds on the inacces- Raven,
sible ledges of the high rocky perpendicular clifl's. Some of the prin-
cipal, localities v/here these birds have nested from ye <.r t« yoai are —
the Roche a Corbeau and "The Canal " on Lake K va, the v/est

side of Lady Evelyn Lake, the Crow Rock in the noitViern part of

! 1

Lofins coni-
niiin.

I .1

nh4

40 I

NIPISSING AKD TEMISCAMING REGION.

!'■

Partridge.
Ptarmigan.

Fish.
Sturgeon.

Habitat.

Trout and
Whitefish.

Annima-nipissing Lake and other places where the cliffs are high and
sufficiently steep. The belted king-fisher {Csryle alcyon) is constantly
seen along the margins of creeks and rivers. The ruflfed grouse or
birch partridge {Bonasa umhellua togata) is very common, as is also
the Canada grouse or spruce partridge ( Dendragapus canaderiois)-
Both the vsrhite ptarmigan (Lagopus lagopus) and rock ptaraugan
{Lagopus rupestris) are also occasional visitors to this district.

Fish are exceedingly abundant in nearly all the lakes. The largest
fish met with is perhaps th.. lake or rock sturgeon {Acipenser rubi-
cundus) although many individuals of the lake trout nearly equal
the sturgeon in size. The sturgeon was formerly » rather abundant
inhabitant of Lake Nipissing, but of late years, owing doubtless to
the increase in the number of settlers, are less common there.

From an economic standpoint, however, the lake trout {Salvelinua
namaycush) and the whitefish (Coregomis clupeiformis) are the most
important, as they are not only abundantly and widely distributed
throughout the larger lakes of the district, but form a usual and
valuable article of diet among the scattered settlements. Both
these fish, although present in considerable quantity in Lake
Nipissing, attain their largest dimensions in the clear depths of
Lake Temagami. There are no trout in Lake Temiscaraing or the
Ottawa River or even in Lake Keepawa, although most of the
lakes immediately tributary to these contain abundant and fine
Brook Trout, specimens of these fish. The brook trout {Salvelinus fontinalis)
although comparatively rare, is rather widely distributed, and it.^ pre-
sence in any stream or lake is a sure indication of unusually clear and
cold water. The small lakes to the west of the Mountain Rapid
on the Ottawa contain them in abundance while they are exceedingly
numerous in the C)pimika Creek and the lakes which this drains,
especially Emerald Lf^'ke. Latour Creek, which empties Tiout Lake,
in the township of Lorrain, on the west sidf of Lake Temi.scaming,
has always been a favourite fishing resort for the inhabitants of the
Hudson's Bay Company's old post, although the largest and finest
specimens of this fish in the whole region may be procured in the
streams entering Willow Island Lake to the west of Lady Evelyn
Lake.

Lake Herring. Closely allied to the whitefish is the fresh-water or lake herring
{Coregonns artedi), which is somewhat abundant in many of the lakes.

Next in importance to the trout and whitefish are the various

species of bass and sunfish which, with the exception of the black

Black bass. bass, do not attain to any great size. The black bass are of excellent

8ARL0W ]

quality t

the lakef

the largi

inoides a]

colour wl

Jakes and

bass hav

water of '

Narrows,

hue is nc

noticed ij

specimens

contains i

bear Net i

list; whil

alJUidant,

The roci
sunfish (Ze,
tions are fa

The comi
allied forms
quality, ia g
while the a\
importance
vitreum), ca
whitefish th-
several wee)
the dee- / ,1
secured in ii
line. At th
the mc f, a!
throughout t
Teniagaiii.
one caugfit b
another from
twenty-seven

Both the c(
onge (iisox 7.
more ■ <adar
the l.ii ,_ V
several I •u-vij
Temiscaming.

.*ff

FAUNA.

41 I

quality and exceedingly plentiful, these fish being found in moat of

the lakes comprised within the area of the map-sheets. Both species>

the large-mouthed and small-mouthed, are present (Micropterus sal-

inoides and M. dolomieu). There is an extreme variability in point of

colour which is clearly owing to the nature of their surroundings. In colour depen-

lakes and streams where the water is of a prevailing brownish tint, the dent on sur-

*^ . roundings.

bass have a correspondingly dark hue, while in the clear, greenish

water of Lake Temagami and Little Lake to the east of the Old Fort
Narrows, the bass have a pale-green coloration. This variation in
hue is not a peculiarity affecting the bass alone, but may be also
noticed in the trout, pike and especially in the pickerel. The finest
specimens of these fish may be secured in Lady Evelyn Lake (which
contains no trout), Temagami, Red Cedar, Annima-nipissing, White-
bear Net and Rabbit lakes, although these by no means exhaust the
list ; while on Lake Temiscaming and Little Lake, though not so
abu .idant, the specimens obtained are generally of verj large size.

The rock bass or red eye (AmblG])lite3 rupeatris) a; id the common Rock -bass and
3unfish (Lepomis pallidus) are also extremely numerous where condi- Sun-fish,
tions are favourable.

The common yellow perch and the pike-perch or pickerel are closely Perch,
allied forms. The yellow perch [Perca americana), although of good
quality, is generally small, rarely attaining over one pound in weight,
while the average size is very much smaller. It is not of economic
importance as a food fish like the pickerel. The pickerel {Slizostedium Pickerel.
vitreum), called by the French, dore, is possibly next to the trout and
whitefish the most valuable food fish found in the region. During
several weeks of summer (<?«nerally in August) these fish retreat to Where Pick-
the dep- / wpter of the lakes, but at other times they may be readily ^'"''^ a'jound.
secured iu iaigi* riu*".".bors either by means of nets or with hook and
line. At the Old F'ort Narrows on Lake Temiscaming, it is by far
the mo. t a!)auda,nt fish. It is also present in most of the other lakes
throughout the di'^^t' let, especially in Lakes Keepawa, Obashing and
Temagani. Th'- general weight is from four to seven pounds, but
one caught by us on White-bear Lake weighed fifteen pounds, while
another from Hunters Lodge Narrows on Lake Keepawa, measured
twenty-seven inches in length.

Both the common pike {Esox lucius) and the great pike or maskin- pike.
ongt5 (Esox nobilior), are found, although the former is by far the Maskinonge.
more i; 'ndant The pike is a very common inhabitant in nearly all
the i I.V s, v'hilc the maskinongt5 is comparativnly rare, although
several i- d-viduals were caught at the Old Fort Narrows on Lake
Temiscaming.

42 I

NIPISSI.VG AND TEMISCAMING RliGION.

Eel, Cat-tiwh
and Chub.

! ;

Good fishing
lakes.

The common eel (Anyuilla rostrata) is also present in many of the
lakey, particularly Temis-'aming and Teraagami. Other fishes which
might be mentioned are deveral species of sucker, the common cat-fish
(Amiurus nebuhsus) and the silver chub (^Semotilus corjwralis) but
none of these are of economic value.

While most of the lakes are very abundantly supplied with fish, there
are some which deserve special mention. Temaganii, Annima-nipis-
sing, Whitebear and Rabbit Lakes are j^ar excellence the waters in
which both trout and whitefish are found in greatest quantity and
best quality, while the bass, pickerel and pike are also of large size and
excellent quality. Lady Evelyn and Temiscaming lakes contain
no trout. The Opimika and Old Fort Narrows on Lake Temis-
caming have always been \A still are excellent fishing places, the fish
chiefly caught being picker. " .ndbass. Pickerel are caught in great
numbers in the spring, abovt :-.m on Lake Keepawa near the outlet

of the Keepawa River, as well c. Hunters Lodge Narrows, while the
Narrows on Obashing Lake is also a favourite resort for these fi^h.

GEOLOGY.

GENERAL STATEMENT.

Gp<>l(if,'ioal The several geological systems and formations represented in the

Subdivisions. rggJQ^ covered by the accompanying map-sheets and subjacent to the

Pleistocene superficial deposits, may be thus stated in descending

order : —

i Silurian — Niagara.
Camuro-Silurian — Trenton.
Birdseye and Black River.

iHuRONIAN.
Laurentian — Diorile-gneiss and granite-gneiss or
" Fundamental gneiss."

The Archa'an rocks of the region here described may naturally be
separated into two great subdivisions, that of the so-called Lower
Laurentian Laurentian and the Huronian, although a few small isolated inliers of
andHuronian. crystalline limestone, and one at least of a dark -gray, exceedingly
sf^ueezed and altered gneissic rock, are found to be inclosed in the
ordinary granitic and dioritic gneisses. These are unimportant in this
district, and so small in area that it has not been possible to distin-
guish them separately on the map. They resemble very closely rocks
which in regions further to the south and south-east are known as the

Arch wan
roclvs.

•ARLOW

Grem
discus
those
in this
the su

Unc

includ(

materii

positioj

a differ

scure ai

sent re|

charact(

by alter

some rej

make ai

later anc

Detail

by varioi

that mos

massive (

been imp

magma o

deformati

complete

been urse

of these r

Every
prefaced 1
to include
molten or
bardeninj:
associated
It must
here repres
just given,
distinct or
rocks as a
they now p
it wjl be 8
wheie a qui

GEOLOGY — GENERAL STATEMENT.

43 1

Grenville series. The present report therefore does not include an}' (irenville
discussion of the relations of the rocks classed as Huronian with ■''"''>*'*'•
those of the Grenville series. These two series do not come in contact
in this area, and the question of their relations is at present being made
the subject of special investigation in central Ontario.

Under the name Laurentian, in the area here described, are Laurcntian.
included a great number of varietal forms of granitic and dioritic
materials, having essentially the chemical and mineralogical com-
position of such rock-types, but differing in their foliated texture,
a difference which although almost invariably present is sometimes ob-
scure and occasionally fails altogether. Their subdivision in the pre-
sent report is based solely on their petrographical and .nineralogical
characters, for although their prevailing foliation, fre:juently marked
by alternating bands of varying composition and colour, resembles in
some respects an original stratification, it has been found impossible to
make any such stratigraphical subdivision corresponding to that of
later and truly bedded formations.

Detailed investigations both in the field and with the microscope, .
by various geologists and petrographers, have of late led to the belief gneisses.
that most of these gneisses have an origin in common with their moie
massive equivalents, and that the prevailing foliated character has
been imparted to the rock-mass by differentiation in a slowly cooling
magma of more or less heterogeneous composition, or as a result of
deformation by pressure after the rock had undergone either partial or
complete consolidation. The cogency of the arguments which have
been urged in favour of the recognition of the greater part, at least,
of these rocks as foliated irruptives now seems beyond question.

Every recent report aiming at scientific accuracy, is necessarily ,j,]^^ ^^^^ ^^
prefaced by an apology or e.xplanation of the use of the term Laurentian the nume
to include such gneissic rocks of irruptive origin, that have been in a
molten or plastic condition at a time subsequent to the deposition and
hardening of later truly stratified rocks with which they are intimately
associated and occasionally interfoliated.

It must therefore be clearly understood that in placing the rocks
here representing the Laurentian at the base of a table such as that
just given, it is not intended to indicate that they stand for any
distinct or prolonged lapse of geological time, nor to aflBrm that these
rocks as a whole, in their present condition, and with the foliation
they now possess, really antedate those of the Huronian system. This,
it w 11 be shown, is not the case in many, if not in most instances
wheie a question of the kind can be determined.

I • .:

:i 1'

1 it

Hi!

^^ ^W7 ° ? ?yffi l'BiB WI "ll

44 I

MPIS8IN0 ANi) TEMISCAMINO REGION.

BARtOW

Origin of
Fundamental

gneiss.

Formation of
granite and
diorite gneiss.

Successive
intrusions.

'"'i'lj.te near
Anikiinii-nipis'
sing Lake.

Granite area
between Rab-
bit and Tenia-
ganii Lake.

The Fundamental gneiss is here therefore accorded a priority in
description to which it is not structurally entitled, a.s it may possibly
represent in great part, the first-formed crust of the earth, which, neces-
sarily thin and fragile, and so liable to frequent upwellings of the
molten mass beneath, has undergone successive fusions and recement-
ations before reaching its present condition. As at present mapped, it
is regarded as a complex of irruptive plutonic rocks, representing re-
peated and intricate intrusions of basic and acidic material. Although
in many instances, and i.i limited areas, the succession of such irrup-
tions can be rascertained, with tolerable accuracy, any attempt to cor-
relate this succession in detail over extended areas, has invariably ended
in more or less complete failure.

In general, however, it may be stated that the earliest secretions of
the magma from which these rocks have solidified consisted of a series
of granitic and dioritic gneisses, very evenly and distinctly foliated,
varying in colour from reddish through reddish-gray and gray, to dark-
green and almost black.

These gneissic rocks were subsequently invaded by a massive, deep-
red biotite-hornblende-guoi i tl;Ht usually possesses a more or less
distinct foliated structure, marked by the parallel alignment of the
bisilicate minerals. It seems highly probable, however, that no great
lapse of time intervened between these successive irruptions, as the
latter in all probability represents the residual portion of the magma,
necessarily more acidic and homogeneous in composition. Dykes of
coarse pegmatite, as well as of fine-grained aplite, cut the diflferent
varieties of gneissic rocks or are frequently interfoliated with them.

To the north-east of Lake Temagami, there is a large area of flesh-
red granite, which in many places, especially in the vicinity of Carry-
ing and Annima-nipissing Lakes, has a distinct foliated structure. In
appearance, composition, and behaviour it has so close a resemblance
to similar rocks mapped as Laurentian further to the south that it is
proposed to include it with these rocks.

Between Temagami and Rabbit lakes, there is a somewhat similar
granite, which, however, is continuous with the main Laurentian area
to the south, and is accordingly designated Vj) the same coloration.
In both cases these rocks pass by insensible gradations into a medium-
textured dark-green gabbro or gabbrodiorite, with which they are
intimately associated, by an increase in the plagioclase and the pre-
ponderance of hornblende as the coloured constituent. Although in
the accompanying map these gabbro masses are shown in the colour
usual for such basic intrusions, it must be borne in mind that they are

believe
that hi

The

and mi

trast, e

ing th(

stratifie

vulcani.'

and str

volcanic

cesses oi

rate wh

member

or round

degrees (

rocks, en

similar n

sericite fi

In earl
dance of
foliation
ficiently i
strata res
granites,
recent yet.
earning, si
general .■•:«
" chloritic
as essentif
been evide
they have
rearrangen
correlated
face in thi
diabase anc
reveals a c
that cannol

Throughf
able into th
follows : — (
slate. (3.)

GEOLOGY — GENERAL STATEMENT.

45 I

believed to represent basic portions or segregations of the same magma
that has elsewhere crystallized as granite.

The Huronian rocks are generally clastic in composition, appearance, Hurouiun
and microscopic structure, and in this respect are in marked con-
trast, even in their most altered phases, to those described as constitut-
ing the Laurentian of the district. A large proportion of these
stratified rocks indicate the existence of intense and widespread
vulcanism, which evidently chaiacterized this period ; their composition
and structure showing a most intimate association of undoubted
volcanic ejectamenta with material resulting from the ordinary pro-
cesses of erosion and sedimentation. The breccia or breccia-conglome-
rate which is so abundantly represented, and here forms the basal
member of the Huronian, is composed chiefly of anj^ular, sub-angular,
or rounded fragments of red and gray granite, diabase of difl'erent
degrees of texture, and various fine-grained slaty and halleflintalike
rocks, embedded in a fine-grained, often argillitic matrix, consisting of
similar material in a much finer state of division, with chlorite and
sericite filling the smaller interstices.

In earlier reports on these rocks, the much greater relative abun- p-^ju. ,„i^co,i.
dance of the granitic fragments, coupled with the so. ^ewhat distinct ceiitions
foliation observable in a few of these, was evidently taken to be suf-
ficiently strong and positive evidence to justify their description as
strata resulting from the degradation of the Laurentian gneisses and
granites. The more detailed and critical examinations made during
recent years, covering the country between Lakes Huron and Temis-
caming, show, however, the error of sich a conclusion in any wide or
general sense. Thus the rock, first described under the name of
" chloritic slate-conglomerate " by Sir William Logan, must be regarded
as essentially of pyroclastic origin, the volcanic ejectamenta having erate.°^"^ ""
been evidently spread out upon the bottom of a shallow sea, where
they have undergone in many instances considerable attrition and
rearrangement by water. Much of the coarser material cannot be
correlated with anything now known to be present at the earth's sur-
face in this region ; while the intimate association of this rock with
diabase and gabbro intrusive masses, rather than with the granites^
reveals a close genetic relationship subsisting between these rock.s,
that cannot be regarded as merely accidental.

Throughout the area, the Huronian, where fully represented, is separ- ^ . , .
,,. , !■• 11... i-i • T 1 Division of

able into three distinct subdivisions which are, in ascending order, as Huronian.

follows: — (1.) Breccia or breccia-conglomerate. (2.) Grayicacke shale or

slate. (3.) Felspathic sandstone or quartzite.

. \

I .i.

!: ,

46 I

NIPISSINQ AND TEMI8CAMING REGION.

Breccia
congloinerato,

(Iraywacke
and ahale.

is: i

Arkose.

Birdseye and
Black River
on Lake

Nipissing.

As a rule, the lowest uumber, or breccia-conglomerate, presents only
obscure evidence of stratification, and wherever such were visible the
rock occurs in thick massive beds, showing only a slight inclination or
dip. This may be well seen in the hills on either side of Lake
Temiscaniing between the Montreal River and the Old Fort Narrows.
Where subjected to pressure, however, as is very frequently the case,
the cleavage-foliation thus developed is a much more prominent
structural feature and is thus very often mistaken for the bedding.
This is especially the case in the region immediately adjacent to Lake
Temagami, where this rock is very widely exposed and where it is
associated with and squeezed between large masses of diabase and
granite.

Superimposed upon this, and forming a transitional rock upwards
into the succeeding subdivision, are beds of varying thicknesses of gray-
wacke or felspathic sandstone, less massive in structure ; while the
coarser fragmental material gradually disappears as an ascent
is made in the series. The succeeding shale or slate, which is in general
very similar in composition to the graywacke or the finer matrix of
the breccia-conglomerate beneath, is often beautifully banded in vary-
ing shades of green, purple or brown. The cleavage in most cases
corresponds with the bedding, although occasional instances were
noticed where cleavage or jointage planes were developed at con-
siderable angles with this bedding. Superimposed on this slate, in
many parts of the area, is a very massive much jointed quartzite or
grit, generally sea-green in colour because of the abundance of
minute scales of sericite distributed through the finer portions of the
rock. Occasionally, however, it has a reddish tinge, and the arkose
then closely resembles a granite, both in composition and appearance.
The rock is so massive that it is often only by the parallel alignment of
certain coarse quartzose and otiier fragments that the original bedding
can be distinguished. These various members of the Huronian here
follow one another in regular and often nearly horizontal succession,
except in the vicinity of the large igneous masses, where they show
considerable evidence of disturbance as well as of alteration.

The Pahvozoic rocks represented in this area consist of outlying
patches of the following formations : — (1) Birdseye and Black River,
(2) Lower IVenton, (3) Niagara.

The outliers representing the Birdseye and Black River formation,
are exposed on some of the islands composing the Manitou group in
Lake Nipissing. These are of very limited extent and consist of sand-
stones, limestones and shales, the whole section probably not exceed-
ing thirty feet in thickness.

MRLOiv. 1

Some SI
overlying
Ottawa R
exposures,
and thus s
occurring

The Nici
light-buflFc
conglomen
slates and
of Lake Te
low, shallo

The coar

sand, are n

surface bei

erratics, esj

paratively s

with coarse

position of

types preva

able distanc

ing, and Tei

district, the

by deposits

is a thick ar

many places

in flats of cc

cut deep anc

plains are st<

strata. In i

of which is o

utilized in th

valleys, and

covered by <

boulders.

In the vici
depth of coai
the gray clay
the vicinity o:
forming flats
have been fo

Bw. 1

GEOLOGV — GENERAL STATEMENT.

47 I

Some small exposures of sandstones and arenaceous limestones occur Trenton
overlying unconfornmbly the gneissic rocks of the Laurentian on the Mattawn.
Ottawa River below Mattawa. The fossils secured from these thin
exposures, indicate that the containing rocks are of lower Trenton age,
and thus somewhat higher in the str.itigraphical succession than those
occurring on the Manitou Islands.

The Niagara formation, as exhibited in this district, is composed of Niagara forni-
light-bufFor cream-coloured limestones and shales, with a basal boulder- Tenilscani'ing
conglomerate, or sandstone, unconformably overlying the Huronian
slates and quartzites on the shores and islands of the northern portion
of Lake Temiscaming. The strata composing this formation form a
low, shallow, synclinal trough.

The coarser varieties of drift material, such as boulders gravel and Pleistocene
sand, are rather abundantly represented on ths higher grounds, the ^P°^''^'''
surface being everywhere more or less encumbered with the larger
erratics, especially on those slopes facing southward, while the com-
paratively shallow and rocky intervening valleys are frequently tilled
with coarse yellow sand, sometimes derived mainly from the decom-
position of rock almost in situ. These boulders are usually of rock
types prevalent in the district, but some show carriage from consider-
able distances. With the exception perhaps of the Mattawa, Nipiss-
ing, and Temiscaming valleys, there is little or no clay present in this
district, the Hatter details of topographical outline being given chiefly
by deposits of coarse yellow sand. In the Temiscaming valley, there
is a thick and extensive deposit of a stiff, stratified, gray clay which in
many places effectually conceals the rock beneath. This clay occurs
in flats of considerable area, through which the various streams have
cut deep and tortuous channels, while protruding through these clay
plains are steep and rocky hills of the prevailing types of the Huronian
strata. In the wide depression the deepest and most northern portion
of which is occupied by the Mattawa River, and which has also been
utilized in the construction of the Canadian Pacific Railway, the minor
valleys, and often too the separating rounded rocky elevations, are
covered by clay deposits containing a considerable intermixture of
boulders.

In the vicinity of North Bay and Sturgeon Falls, a considerable
depth of coarse and yellow sand is present at the surface, concealing
the gray clay beneath ; but to the west of Sturgeon Falls, especially in
the vicinity of Verner, the stiff, gray, stratified clay comes to the surface,
forming flats which have been burnt over or cleared. So far no fossils
have been found in these clays, although in places diligent search

^ ^

1 ;■ I
, '1

■I .;. i
■ I

48 J

NIPISSINQ AND TEMISCAMINO REGION.

Are s covered
by (liffcreiit
rock forma-
tion».

was made for any such evidence of their origin, especially in
the hard concretionary nodules which may be occasionally noticed.

The areas covered by the several rock-formations maj' be stated
roughly as follows : On the Lake Nipissin;,' sheet there are about 3186
square miles of Laurentian, and 270 scjuare miles of Huronian, while
on the Lake Temiscaming sheet there are only 946 square miles of
Laurentian, 2470 square miles of Huronian and associated eruptives,
and forty square miles of Silurian. The two sheets combined there-
fore show 4132 square miles occupied by Laurentian, and 2740 square
miles by Huronian and associated granites and diabases. The Silurian
covers about forty square miles, but extends north-westward to a con-
siderable distance beyond the northern confines of the Lake Temis-
caming sheet. The aggregate area of Cambro-Silui'ian strata exposed
on Tiake Nipissing and Ottawa River is less than two square miles.

Laurentian.

Origin of name The name Laurentian was originally proposed by Sir William Logan,
in 1853, as the most appropriate designation for rocks classified by
him in previous reports as the " Metaraorphic Series," and which
were believed to be identical in composition and origin with similar
rocks so named and described by Lyell. The term thus introduced
soon received an almost universal adoption by geologists, as a conveni-
ent one for the gneissic crystalline rocks found to underlie unconform-
ably the Palseozoic strata, and presumably forming the oldest of the
geological systems. The urgent need of such a distinctive appellation
was recognized as a consequence of the ambiguity which would neces-
sarily arise from the use of such a general term as "metamorphic,"
which is applicable to any group of strata in an altered condition,
while the peculiar fitness of the name was suggested by the fact that
these rocks were found to constitute the bulk of the Laurentide moun-
tains, a series of elevations lying to the north of the River St. Law-
rence, and which were so called by the late Mr. Garneau, the historian
of Quebec.

Griffin of term The term "gneiss" or "gneuss" was originally employed by the
"gneiss, early Saxon miners for the country-rock containing the Erzgebirge silver

ore deposits The rocks so named were divided into a " red " and
" gray " variety, which although differing somewhat in their component
minerals presented many features in common that caused them to be
included under a uniform designation. The rocks so described are
closely analogous in composition and structure to many of the rocks

Urgent need
of name.

•AHLOW. '

within

"gneis

adopte*

tially ^

solely (

pecuJiai

differen

howevei

variety

but whi(

parallel

Althoi
inapplica
except as
examinee
term, as i
microscop

The ori

more or It

mulgation

Hutton ar

definition

primeval c

sedimentai

been remoi

Such rocks

mental gne

upon whic

Metamorph

the most pc

structure ar

internal hea

The vario

a long time

while masses

unyielding tc

the most pro

to be entirelj

allied rocks,

surviving tra

which had e

•]

LAURENTIAN.

49 I

within the area of the present map-sheets, and to which the name
"gneis.s"has been usually applied. The name was very generally
adopted hy geologists, and its use was primarily restricted to rocks essen-
tially granitic in their composition and appearance, differentiated
solely on account of their foliated texture ; the persistency of this
peculiar structure over large areas, presumably furnishing proof of a
diff'erence in origin from the normal or massive type. Gradually, I'^e of term
however, the use of the term became so extended as to include a great
variety of crystalline rocks differing widely in composition and origin,
but which exhibited in connnon a more or less decided tendency to a
parallel arrangement of their component minerals.

Although modern petrographical studies have demonstrated the (fueiss useful
inapplicabilitj' of such a term for purposes of accurate description, '/ield'teVin!!''^'^^
except as an affix to denote the structural features of the rock-types
examined, the name must still be employed as a convenient " field "
term, as a means of rough description anc' correlation, where detailed
microscopic examination is either impossible or considered unnecessary.

The origin of these gneissic crystalline rocks was, for a long time, ( )riKin of cry-
more or less a matter of theory and conjecture. Previous to the pro- '
mulgation of the theories regarding rock metamorphism, first held by
Hutton and subsequently by Lyell, to whom we owe the first use and
definition of this term, these rocks were regarded as portions of the
primeval crust, which had either never been enveloped by the later
sedimentaries, or from which such covering, if originally present, had
been removed as a result of subsequent upheaval and denudation.
Such rocks were then almost invariably referred to as the " Funda-
mental gneiss or granite " and believed to be the basement or floor
upon which all subsequent sedimentary formations were deposited.
Metamorphism, either regional or contact, has always been considered
the most potent influence in the destruction of evidences of original
structure and composition in rocks subjected to the effect of the earth's
internal heat, or that engendered by the proximity of eruptive masses.

The various changes, however, which this term describes, were for Met-

a long time thought to be confined entirely to sedimentary strata, }j,',',i,

while masses of igneous plutonic rocks were regarded as too hard and ""^nt'ii'y rocks

unyielding to be at all affected by the metamorphosing agencies of even

the most profound orographic movements. Foliation, though long held KoHivtion dis-

to be entirely distinct from stratification in the case of slaty and other t'^ctfro™.

*' _ _ "' stratitii'ivtion.

allied rocks, was in the instance of these gneissic rocks regarded as the
surviving traces of the parallel structure due to original sedimentation,
which had escaped obliteration. It is only in very recent years
4

■ fon-

ledi-

\i :

> i?

>' I

Work by
LoHReii.

Work by
Lehmann,

50 I

NIPI88WO AND TEMI8CAM1N(1 UEOION.

Daubree's
opinions.

Results of
work by Niiu-
mann and
Reusch.

Work by Ten! 1
and I Williams.

that this impro.sHion has been overcome by detailed examination and
study, both in tiio field and with the micro.scope, carried on by many
individual observers in large and widely separated districts, showing
clearly that foliation and schistosity cannot be assumed to denote
original stratification.

The first really exact and satisfactory account of crystalline schists
resulting from the nietumorphism of massive eruptives, was given as
the outcome of the detailed work by Loss^n in the Hartz Mountains,
who, as early as 1872*, directed attention to the deformation of diabases
occurring in contact with granites, and showed the close analogy
existing between the results of contact and regional metamorphism, as
well as the production by metamorphic agencies of a foliated structure
not connected in any way with stratification.

The most important contribution, however, iu regard to the effects
of dynamic metamorphism, appeared in 1884, from the pen of Prof.
Johannes Lehmann, who after several years detailed studies on the
origin of crystalline schists, based on a very large number of observa-
tions, made chiefl}' in Saxony, but also in Bavaria and Bohemia, pub-
lished his celebrated memoir on this subject.! The conclusion is reached
that "gnt'iss" is simply a structural form of granular felspathic rocks,
and as such is capable of subdivision according to composition into
varieties corresponding with the types of the ordinary massive
plutonics, while the prevailing parallel structure may be,but very rarely
is, original. He regards these foliated rocks as of igneous origin and
not in any way related to sedimentary deposits, the characteristic
structure being developed as a result of " stretching " when the rock
was in a solid state. It is further concluded that such rocks become
more evenly and finely banded in proportion to the intensity of such
" stretching " action.

Daubr^e was also convinced that the schistose and foliated structures
frequently assumed by massive rocks was not connected with original
stratification, but secondarily developed as a result of pressure before
the rock had wholly solidified. JNaumann emphasizes this latter fact,
while Reusch, from studies undertaken in the vicinity of Bergen in
Norway, also comes to similar conclusions. In England, Teall, from
his examination of the metamorphic area in the vicinity of the Lizard
in Cornwall 1 1 reaches results closely resembling those of Lehmann j

*Zeit8chr. Deutsch. Geol. Gesell. vol. XXIV, p. 763, Berlin, 1872.
fUntersuchungen iiber die Enatehung der Altkrystalliniachen Schiefei-gesteine.
Bonn, 1884.

JEtudes synthetiques de geologie Experimentelle, p. 432. Paris, 1879.
liGeol. Mag., Nov., 1886.

MMOW,

while ii

Marylar

and Ma

has shov

ginally u

ation an(

Lake dis

various :

were larg

under an

viscid, col

plained a«

ing or def

Previou
morphism
sunken str
by Lyell ai
world-wide
in the desii
events as r
should hav(
itteating th
-at revealir
crust, asaci
wellings of
a series of
part of fol
denudation
outward res
undoubted
which were 1
ation ; as we
abundant rea
resented by t
intimate asso(
have originate
also cited as a
sediments. S
most classic b

*Bull. U. s.
tAnnual Rep

MMOW.

LAURENTIAN.

51 I

while in the United States, in the gahbro area near Baltimore,
Maryland, as well as in the greeustone-achist area of the Menominee
and Marquette regions in Michigan, tlie late Prof. Geo. H. Williams
has shown the secondary development of a schistose structure in ori-
ginally massive plutonic rocks.* In Canada, Lawson,t from his examin- ^V^^k by
ation and studies of the rocks of the Lake of the Woods and Rainy
Lake districts, was the first to draw attention to the fact that the
various foliated crystalline rocks usually classified as Laurentian,
were largely plutonic rocks, which have crystallized slowly, probably
under an extremely gradual diminution of temperature, from a thickly
viscid, coherent or tough hydrothermal magma. The foliation was ex-
plained as a result of " differential pressure which by causing a yield-
ing or deformation, induced a flow in the mass."

Previous, however, to the appearance of these results, the nieta- Metamor-
morphism of sedimentary rocks occurring " as deeply buried and
sunken strata " had been so clearly described and so strongly advocated
by Lyell and others, that their views gained an almost immediate and
world-wide credence and adoption. It is therefore not surprising that,
in the desire to trace back as far as possible the sequence of tr ^logical
events as revealed by the accumulation of stratified deposits, there
should have been included at the base a complex of crystalline rocks
ittesting the presence not of conditions favourable to sedimentation
.at revealing the early unstability of the necessarily thin and weak
crust, as a consequence of which it was probably peculiarly subject to up-
wellings of the molten mass beneath. The ultimate result being
a series of immense batholitic intrusions, composed for the most
pait of foliated plutonic rocks, which subsequent upheaval and
denudation have revealed at the present surface of the earth. The
outward resemblance of these foliated or gneissic rocks to certain Restunblance
undoubted clastic rocks, present in later geological formations, gtiiititied
which were known to have undergone extensive deformation and alter- ''"''^^•
ation ; as well as their interfoliation with truly bedded rocks seemed
abundant reasons for their classification as one uninterrupted series rep-
resented by this immense accumulation of stratified material. Their
intimate association with crystalline limestones, which were believed to
have originated in much the same manner as later calcareous strata, was
also cited as additional evidence of their depoi'tion as ordinary aqueous
sediments. Subsequent work in the county of Argenteuil, rendered al-
most classic by the detailed labours of Sir William Logan, as well as

*Bull. U. S. Geol. Surv.. Nos. 28 and 62.

fAnnual Report Geol. Surv. Can., vol. I., (N.S.)., Part c, c, 1885.

52 I

NIPiaSINO AND TEMISCAMINO RKOION.

Difficulties at-
tending first
examinations.

Use of micro-
scope.

in other extensive areas of Arch-Tan rocks in Canada, have since shown
the fallacy of many of the conclusions then reached, and both Adams
and Ells are firmly convinced that the undoubtedly clastic rocks pre-
sent in the area usually considered as " typical " of the Laurentian, form
but a small proportion of the rocky complex, while they are
associated with and inclosed by much greater volumes of ^jneissic
rocks closely allied in petrographical characters to granite, diorite and
gabbro.

In the early years of the Canadian Geological Survey, the advance
of accurate and detailed information regarding these rocki was greatly
retarded for iseveral very obvious reasons. In the first place, by far
the larger portion of the country characterized by the presence of such
rocks v/as a vast almost uninhabited wilderness of forest. The only
access to such regions was by means of canoes, through obstructed and
often little known routes of travel. These conditions have in a great
many instances been improved of late years by the gradual settlement
of the country and the necessary construction of roads. In the i-econd
place, great difficulty was fo.' a long time experienced in obtaining
trained and reliable observers competent to deal with the mtmy diffi-
cult and complex problems presented. Sir William Logan, when
carrying on his work in this connection, was often forced to depend for
information covering many essential details, on observations by men
scarcely possessed of the requisite qualifications.

Thirdly, the extreme metamorphism and deformation to which all
such rocks had presumably been subjected on account of their very
great antiquity, and the absence of any known methods by which their
original minute structures and mineraloj^ical composition could be
deciphered, presented seemingly insuperable barriers to the complete
and satisfactory explanation of tneir origin. In the fourth place, the
very natural assumption that such rocks represented extremely meta-
morphosed sediments, and the consequent application of the ordinary
methods of geological research made use of in the much later and
typical stratified deposits, served only to aggtavate the difficulties
already existing.

The adoption of the microscope for petrographical research removed
the main difficultier attending a satisfactory study of these rocks,
m.arking an era in geology, since which time the progress in exact
knowledge has been rapid. In fact, i\:^ accumulation of reliable in-
fofraation connected with this long-debated subject has already assumed
saoh large proportions that many geologists look hopefully forward to the
time when we ehail prooably possess an even more complete knowledge

LAURENTIAN.

53 I

of these rocks and their manner of formation th&n we now do of many
more recent rocks.

In 1844, when Logan decided l.o make an examination of the region 'iogan'a work
bordering the Ottawa River, he found a mass of foliated crystalline 'Kiver.*"*
rocks that seemed to him capable of subdivision into two conform-
able series, although in this as well as many succeeding reports, he
included them under the one group, which he subsequently called
Lower Ll. arentian. The lower or older series consisted exclusively
of "syenitic gnpi-is showing no end to the diversity of arrangement
in which the minerals and the colours will be observed, but there id a
never failing constancy in respect to their parallelism. But this
though never absent is sometimes obscure." These rocks were sup- Sulxlivision
posed by Logan to occur in the form f>f a low anticlinal arch in the .,,i(j Lower
region extending from the Mattawa River to the vicinity of the com- I-iiiurentian.
bined mouths of the Montreal and Matabitchouan on Lake Temiscam-
ing. The upper series is stated to crop out in the district fo the
south of the Mattawa and Ottawa rivers and to be characterized " by
the presence of important bands of limestone which have undergone
extensive cystp-llization as a result of extreme metamorphism," while
the various gneissio rocks which separate the several bands of limestone
"differ in no way either in constituent quality or diversity of arrange-
ment from the gneiss lower down."

Subsequently, this lower gueiss was called the " Ottawa Series,'' Ottawa and
while the upper group, diflferentiated solely in the tirat place on account gj^"j^' ^
of the presence of the limestones, was included under the name Middle
Laureiitian or Grenville Series. The name Upper Laurentian was Upper Lau
given to a terrane formed chiefly of anorthositos which were after- ^"^ '' ""
wards shown to be of irruptive origin, and with which were classified
by mistake certain gneissic and limestone bands, identical in char-
acter with those included as the Grenville Series and to which they
clearly belong.

In the district therefore covered by the Nipissing and Temiscaming
sheets, the rocks to be described would, under the old classification, have
been included as Lower Laurentian, although in the area to the south
of the Mattawa River, precisely similar gneissic rocks, because of their
inclusion of small isolated patches of crystalline limestone, have usually
been described as of Grenville or Middle Laurentian age. These
patches of crystalline limestone are only very occasionally present and
are evidently caught up by and embedded in much greater volumes of
gneissic or foliated rocks here of truly igneous origin. In such a way
as to point to the conclusion that in tliese limestones we may have

i i

1 5

;(■',: ;-

iT.

54 I

NIPIdSING AND TEMISCAMINO BKGION.

Use of torni
Laurentiaii.

Two groups of
gneisses.

' i^

small remaining portions of a sedimentary series, which, although
highly altered, have not been wholly absorbed by ihe surrounding foliated
material.

The term Laurentian, as applied in connection ■vith the map-sheets
here under description, therefore includes only such granite and diorite
gneisses as are usually characteristic of this ancient complex.

The gneissic rocks exposed throughout this district fall naturally
into two great groups.

. An acidic group : — consisting of those foliated rock- similar in
composition to granites, etc., to which they correspond, their
differentiation being determined solely by their foliated tex<^' -'
which usually pronounced, is sometimes obscure and occasioi ,y
altogether absent.

II. A basic group : — These rocks occur interbanded with the more
acidic gneisses and represent either basic segregated portions of
the granite magma, or foliated basic irruptives allied to diorites,
diabases, etc., caught up in it.

The results obtained from the detailed petrographical examination
of the large number of thin sections prepared from typical specimens,
specially selected as representing all the observed varieties occurring
in the region, coupled with extended observations concerning their
field relations, has furnished the most convincing proof that the vast
majority of such rocks may be referred to some type of irruptive mat-
erial. On the other hand, those gneisses whose origin may be in doubt
and which are in some cases held to be sedimentary, constitute an ex-
--. . . , ceedingly small proportion of the whole series. In fact, the results
Sir A. lieikie. obtained from the examination and study are very closely analogous to
the conclusions arrived at by Sir Archibald Geikie regarding similar
old rocks exposed in the British Isles, who says : "These rocks are in
the main various forms of eruptive material ranging from highly acidic
to highly basic ; they form in general a complex mass belonging to
successive periods of extrusion ; some of their coarse structures are
probably due to a process of segregation in still fluid or mobile, pro-
bably molten material consolidating below the surface ; their granulated
and schistose character and their folded and crumpled structures point
to subsequent intense crushing and deformation ; their apparent alter-
nation with limestone and other rocks which are probably of sedimen-
tary origin are deceptive, indicating no real continuity of formation,
but pointing to the intrusive character of the gneiss."

CARLOW. ]

The(
charact(

1. Cc
the ider
known
many c;
local we
f>hism.

In ord
gneissic
study in
the Lab(
are the n

Silica

Alumina

Ferric oxide
Ferrous oxic
Manganous t
Lime . .
Magnesia .
Potassa . .

Soda

Water at ioo
ir above

Tota

I. Grani
in previous
toid gneiss
massive anc
parallel disf
and only ve
all continuo
quartz, witl
sericite, chh

"Annual Re

•]

COMPOSITION OF GNEISSES.

01) I

The chief facts which together seem to prove the originally igneous
character of the rocks above referred to may be stated as follows : —

1. Composition of the gneissic rocks. — The microscope reveals at once
the identity of these in mineralogical composition with the different
known varieties of granite and diorite, the constituents present, in
many cases, showing little or no alteration, except that produced by ^f gneisses.
local weathering, or as a result of somewhat limited dynamic metambr-
^hism.

In order to ascertain whether the chemical composition of these
gneissic rockd would bear out the conclusions derived from their
study in the field and under the microscope, six analyses were made in
the Laboratory of the Survey by Mr. F. G. Wait. The following
are the results : — *

\n. ^\

Silica

Alumina

Ferric oxide

Ferrous oxide ... .
ManganoHs oxide. . .

Lime

Magnesia

Potassa

Soda

Water at 100° C . . .
„ above 100° C.

Totals... .

71 CO

14-84

1-25
tr.
103
0-37
7 00
3 13
OlO
0-49

II.

"6
a
he

III.

(59-39
17 -40

99-99

1-38

"2-14'
0-52
2-77
518
0-00
0-47

a
to

07-74
1(;-13
1-.00
l-9()
tr.
4-41
1-30
1 30
4-92
0-10
0-80

IV.

a
tc

S i
■S.2

Analyses.

99-37 100-28

07-50

66-94

44-92

18-23

17 -84

18 88
2-73

2-39

4-30

13-76

tr.

0-26

1-85

1-8G

9-07

1-56

1-82

5-38

4-25

3-36

0-53

3-79

1-85

2-94

0-08

015

0-20

0-90

1-75

1-62

100-55

99-87

100-29

I, Granitite-gneiss from west shore of Taggart Bay, Keepawa Lake —
in previous reports usually referred to as red orthoclase gneLss, grani-
toid gneiss or gneissoid syenite. The rock is of a deep flesh-red colour, I'esmption of

r .... i/.].-!. gneisses,

massive and granitic in appearance, the foliation being imparted by the

parallel disposition of the coloured constituents. It is highly felspathic
and only very occasional thin bands of basic material occur which are at
all continuous. It contains much microcline, orthoclase, plagioclase and
quartz, with much smaller quantities of biotite and epidote, Sphene,
sericite, chlorite, apatite, allanite and zircon are present as accidental

•Annual Rei>ort, Geol. Surv. Can., vol. IX., (N.S.) Part R., pp. 18-20.

'hi

56 I

NIPIbSING AND TEMISCAMING REGION.

3I '

m i

Description of or secondary minerals. The rock has evidently been subjected to con-
analysed, siderable pressure. The felspar and quartz have often undergone
advanced granulation, while the surviving large individuals exhibit
marked Lndulous extinction. Microcline, as might be expected, is
abundant, as also areas of granophyre.

II. Granitite-gneiss from south shore of McLarens Bay, Keepawa
Lake. This was selected as representing the light reddish-gray granitic
genisses so common in the district. The hand specimen shows a light-
gray, rather fine-grained micaceous granitic rock, tinged with red oxide
of iron, and showing only indistinct foliation. Composed of orthoolase,
microcline, plagioclase, quartz and biotite with a little apatite,
zircon, sphene, magnetite and occasional minute individuals of secondary
muscovite and epidote. The biotite sho%vs a slight alteration to
chlorite in some instances and occurs for the most part in small isolated
plates, possessing a rude parallelism and rarely aggregated together.
It shows only slight evidence of pressure.

III. Granitite-gneiss from west shore. Lake Temiscaming at north
end of Opiraika Narrows. A good average sample of the ordinary
so-called gray-gneiss. Macroscopically, this is a very distinctly foliated
rock, the foliation being produced by alternating bands of light and
dark-gray colours. The darker bands are composed almost wholly of
the coloured constituents while the light-gray portions are made up
chiefly of quartz and felspar. The thin section shows quartz, orthoclase,
plagioclase, biotite and epidote as the principal constituents. Epidote
and titanite are common inclusions in the mica.

IV. Granite-gneiss from the north-west shore of Leonard Inlet, Wick-
steed Lake. The hand specimen shows a rather coarse-grained, grayish,
indistinctly foliated rock, much stained with yellowish-brown iron
oxide and showing large phenocrysts of white orthoclase. The chief
minerals present are orthoclase, microcline, plagioclase, quartz, biotite
and muscovite. Apatite, zircon, epidote, zoisite, allanite 1 and pyrite
were also noted in very small quantities. The rock has evidently been
subjected to considerable dynamic action. The muscovite is primary
intergrown with perfectly fresh reddish-brown biotite.

V. Cyanite-granite-gneiss from the east shore of the Ottawa River,
half a mile north of Snake Creek. The hand specimen shows a coarse-
grained granitic rock with a distinctly banded structure caused by
layers rich in biotite, alternating with layers of quartz and felspar
comparatively free from that mineral. The distinctive feature of the
rock is the abundance in portions of it of a light, to deep-blue cyanite,
in large columnar individuals, some of which are half an inch across
and an inch in length ; garnets of a deep pink colour are also plentiful,

■ARIOW.

]

COMPOSITION OP GNEISSES.

57 I

and some individuals are as much as half an inch in diameter. Under
the microscope the rock is seen to be composed of orthocla.se,plagioclase,
quartz, biotite, cyanite and garnet with smaller quantities of muscovite,
graphite, titanite, zircon, apatite, pyrite, pyrrhotite and epidote. The
rock is typically holocrystalline and granitic and shows no extreme
evidence of granulation.

VI. Quartz-mica-diorite-gneiss from Ottertail Creek, lower end of
the 2nd portage above the junction with the north branch. In the
hand specimen this is a dark-gra}-, almost black, glistening, evenly
foliated rock stained in places with iron oxide. lb is composed of plagio-
clase, orthoclase, quartz, hornblende and biotite, with sphene, apiitite, zir.
con, pyrite, magnetiteand limonite as accessory minerals. The hornblende
is much more abundant than the biotite. The evidence of pressure is
very limited. The rock constitutes the dark basic bands so character-
istic of exposures of the gray gneiss.

Time would not permit of the separate analysis of each rock-type

included in the accompanying table, and therefore no attempt can be <^/neral result

t J 's > r of examiationa

made to institute comparisons in detail with the published analyses of
granites and diorites. Sufficient has been done, however, to show
somewhat clearly that in general these foliated rocks bear a close
analogy in chemical composition to their massive equivalents, while on
the other hand, they are quite different in this respect from any rock
resulting from ordinary processes of sedimentation. As Dr. Adams
remarks,* the points of distinction and those which mark them as of
igneous origin are, high silica, combined with low alumina and big.,
percentage of alkalies. The lime also, as is usually the case in granites,
is in excess of the magnesia. It would seem, however, that the granite-
gneisses, as a rule, are more basic than their massive equivalents,
although presenting an equally wide range in their silica contents.
The decrease in silica is accompanied by an increase in tht alumina,
while soda tends to exceed potash in the more basic varieties thus
marking a passage to the gabbros and diorites. The high percentage
of alumina with low alkalies noticed in No. V. is due to the presence of
cyanite, but otherwise the composition is essentially similar in every
other respect to the ordinary granitites of this and other Archican
districts. There is as is usual in granites, the preponderance of
lime over magnesia which though slight in this case, is nevertheless
in marked contrast to the sillimanite gneisses described by Adams*
where the magnesia is often nearly three times as abundant as the
lime.

i hi >

A W 1

:il!^

"Annual Report, Geol. Surv. Can., vol. VIII. (N.S.) Part J, p. 44.

■ n

58 I

NIPISSING AND TEMISCAMING REGION.

|-Si

:i-,

i !

^It

•) '

The quartz-micadioi'ite ^VI.) is analogous in chemical composition
to the most basic phases of the gabbros and diorites. The hornblende
and biotite are much more abundant than the felspathic constituents,
while quartz is only very sparingly represented.

Structure.!. 2. Microscopical structure. — The various thin sections examined,

show unmistakfcbly the holocrystalline structure so characteristic of
granite, diorite and gabbro, the felspar and quartz individuals forming
comparatively large areas of interlocking grains, especially in the more
acidic portions or bands in the rock, with which are associated the
hypidiomorphically developed bisilicate constituents. There is no sug-
gestion whatever, in the great majority of such rocks, of the
secondary enlargement which in certain arkoses and quartzites pro-
duces a somewhat similar interlocking arrangement, as the rocks have,
in many instances, been subjected to but limited metamorphic action.
The foliation, which is the differentiating characteristic of these rocks,
is often so coarse that it is only apparent in large specimens or some-
what extended exposures of the rock. This parallelism is, therefore,
often indistinguishable with the microscope, so that in the thin sections
the resemblance is complete between foliated and non-foliated varieties
of such essentially similar mineral aggregates.

At the present day, fused magmas are regarded as a more or less
complex solutions, which, by reason of their high temperatures, obey
the same laws in the order and method of their solidification as those
which govern the crystellization of ordinary solutions of a similar
Order of heterogeneous composition. Thus, in the numerous thin sections

generation. examined, a certain general and definite order is observable in the
generation or crystallization of the various component minerals that has
been rather closely adhered to in the progress of consolidation. In this
manner zircon, sphene, apatite and primary epidote, which are the first
to form in the slowly cooling mass, are almost invariably present in
shapely outlined and well developed crystals, evidencing considerable
freedom from restraint during the progress of their formation.
The various iron ores which may happen to be present, are of earlier
generation than the coloured or bisilicate individuals, which latter
are usually present with hypidiomorphic outline, although occasional
individuals often show sharp and well delined crystallographic bound-
aries. The customary grouping together in masses or nests of such basic
material, produces a mutual interference of the constituent individuals
which militates greatly against perfection of crystal boundaries. The
various apatites, sphenes, etc., which are the first minerals to form in
the cooling rock-mass, usually occur, as might be expected, either

4. Jjij
line of ju
doubted
and detai
between
which Jat
gneissic rt
respect to

BARLOWc

]

COMPOSITION OF GNEISSES.

59 I

embedded in, or in close conjunction with such ferro-magnesian con-
stituents, although the rest of the rock, while much poorer relatively
in such minerals, m<ay not be entirely free from them. The felspar and
quartz, which are the last to solidify, occur in more or less irregular
areas, usually elongated in the direction of thr* foliation, or showing,
especially in the case of the quartz, that the residual spaces existent in
the rock-mass were already of this form and character.

3. Macroscopical structure. — The various dark and light-coloured Field rela-
bands of relatively greater or less basicity, succeed one another across
the strike or cut one another oif, thus suggesting, even to a casual
observer, a complicated intrusion of one portion through another,
although the frequent absence of any distinctly recognizable boundary
between the different folia shows clearly that such conditions obtained
in the mass long before its final consolidation. Although especially
when arranged in approximately horizontal position, the alternation of
such bands resembles somewhat closely the parallelism produced by the
alternatinji; sequence of stratified material of diflfering coarseness and
composition, a closer inspection shows that there is no evidence what-
ever of the sorting and reai'rangement by aqueous agencies so char-
acteristic of all sedimentary strata. The tendency to nuclear aggre-
gation observed in the crystallization of the first-formed constituents,
seems to be a usual and marked feature, not only of slow cooling magmas,
but of all highly saturated and complex solutions when undergoing
change to the solid state. It is therefore quite evident, both from
macroscopic and microscopic examination, that perfection of foliation is
reachel in these gneisses when, during the process of cooling,
accompanied by differential movements, the pressures produce
a kind of flow in the still mobile mass, thus tending to the
parallel disposition of the various bands or masses of differing com-
position. The viscosity of the whole was such as to prevent the too
free transmission of the material of contiguous bands or portions, thus
furnishing the approximately sharp lines of division so frequently
observed.

I i'

:i : 1

4. Junction with overlying rocks. — The immediate contact, or
line of junction, with originally overlying clastic rocks, reveals un-
doubted evidence of the irruptive character of the gneisses. Numerous
and detailed observations have been made of the line of demarcation
between these Laurentian gneisses and Huronian slates and quartzites, Laurentian
which latter are of undoubted clastic origin. The behaviour of the '"t'^sive

. . . . through

gneissic rocks under these circumstances, is precisely similar in every Huronian

respect to that which obtains in the case of granite, intrusive through

'j^"'"

60 I

NIPI8SING AND TEMISCAMING REGION.

', J

.; !

Two kinds of
foliation.

neighbouring bedded strata. Detailed descriptions have already
appeared* regarding the various contact phenomena witnessed along
the line of junction between the Laureritian and Huronian, embracing
not only this region, but also the district to the south-west included
within the area of the Sudbury and French River map-sheets
(Nos. 130 and 12.5, Ontario). The facts there noted, and since borne
out by more extended observations, show distinctly that the gneisses
are intrusive in the Huronian, and are, therefore, in their pre-
sent form younger than the elastics which they invade. Although, in
places, a seeming transition exists which might be mistaken for an
alternating sequence of stratified material, the relations thus observed
find their true explanation in the presence, at these places, of a zone
of varying thickness formed by a commingling of the sedimentary
material with the igneous rocks, as a result of actual fusion, or by the
presence of a series of more or less parallel dykes piercing these elastics.

The foliation presented by the.se rocks isof two distinct kinds, although
there is almost every possible gradation between these two extremes.
It may consist of the parallel arrangement of certain of the constituent
minerals, usually the bisilicates, but sometimes also the porphyritic fel-
spars, or it may be due to an alternation of lighter or darker bands,
showing a varying chemical and raineralogical composition. Intermedi-
ate phases of such structures are produced by the development, in more
or less approximately parallel po:3ition of nuclei, or nests, of the ferro-
magnesian constituents, whose gradual coalescence into ever-lengthen-
ing bands, produces ultimately that perfection of foliation actually
found.

The foliation just described, is the one characteristic of the more
massive and granitoid varieties, included under the first or acidic
group, and is evidently the result of the application of pressure to a
magma of somewhat homogeneous conipo.sition. On the other hand,
the second variety of foliation is produced by alternating sequences of
rocks belonging to both acidic and basic groups, and has l)een imparted
to the rock-mass as a result of differentiation in a slowly cooling magma
of heterogeneous composition, aided by a flowing movement in a more
or less constant direction.

„ ,. . The results obtained by the microscopic esamination indicate, in the

Foli.ation pro- . . , , i , i . ,, ,

duced when most positive manner, that the banded structure so universally observ-

mrtiailv con- ^^^® "'^ *'^^^ rocks, was imparted to the whole mass while still in a
solidated. molten, or, at most, only partially consolidated condition. One of

*American (icologist, vol., VI., \t]). l!)-32 (July, 1890), also Bull. (Jeol. Soc. Am.,
vol., IV., pp. .313-382.

fore it

COMPOSITION OF ONKISSES.

61 I

T (I

the most significant facts noticed in this connection, is that many of
the moat markedly foliated gneisses show little or no trace of having
been subjected to any great degree of deformation ; nor is there any
reason whatever to suppose that the rocks so examined have undergone
such recrystallization as to mask the evidence of such action, if any
previously occurred. In many instances, it is equally certain that sub- Klircts nf dy
sequent dynamic action has, after the complete solidification of the
magma, somewhat modified and accentuated such foliation, but even
in these cases, there is every reason to believe that pronounced parallel-
ism previously existed as a primary structure of such lOck-masses^
before the ai>plication of pressure.

The somewhat uniform direction in strike of this banded structure, I'lnfomiity of
over the larger portion of the area covered by the accompanying map- *■'"'•
sheets, and its marked correspondence indirection with the line of out-
crop of the neighbouring stratified Huronian rocks, seem to point to
the conclusion that the resistance off'ered during the irruption of these
gneisses by such hard strata, has been the irtain determining feature of
the direction of foliation. During the progress of this igneous invasion,
the forces of upheaval acted along certain definite lines or centres,
thus producing irregular ovoid forms, often of great area, the inner Snuctmal
portions of which are now occupied by comparatively fiat-lying gneisses,
or, in occasional instances, by more massive or granitoid varieties, sur-
rounded by an outer border or zone where the foliation becomes
much more pronounced. In certain instances, where the dome-like
structures thus produced have been denuded, and are of limited extent,
a great diversity exists in both the direction and angle of dip of the
foliation within a comparatively small area, but where, as is usual
thoughout this district, these ovoid areas are of great size, the direction
of foliation shows a corresponding increase in uniformity.

Intimately associated with these gneisses and granites, are certain
portions, often of themselves constituting considerable and there-
fore important rock-masses, which, on account of certain peculiarities of
composition, as well as from their structural relations with the surround-
ing rocks, have been commonly referred to as " pegmatite," and which by ivgtnatite.
reason of their usually coarse crystallization have been sometimes
called "giant granite." Haiiy first applied the name pegmatite
to the intimate admixture of orthoclase and quartz, also known as
graphic granite. Later, Naumann extended its u.-e to include all the
coarse varieties of muscovite-granite, vein-like in appearance and fre-
quently containing tourmaline. Subsequent writers, as detailed inves-
tigations into its composition and origin proceeded, have still further

.' J'

mi:

62 I

NIPISSINQ AND TEMISCAMINO RRGION.

widened its use, until, at the present day, the employment of the term
in connection with that of the parent plutonic mass with which it is
associated is necessary, before any definite idea can be formed of its
Ufle of terms, precise mineralogical composition. In petrography the terms micro- and
macro-pegmatite have always been used in a structural sense only, to
denote those intergrowths of quartz and felspar, or of two differing species
of felspar which are sometimes characteristic of occurrences in rocks of
these minerals. Thus the various plutonic masses of syenite, diorite,
gabbro and diabase, may each have their individual pegmatitic equi-
valents, representing the final product of their solidification, although
the abundance of such aggregates in connection with these
rocks is much less than in the case ot granites. This com.
parative iufrequency is perhaps most adecjuately explained by
the relatively much greater basicity of such rocks, their more rapid
rate of cooling, as well as the comparative scarcity, throughout the
greater portion of the mass, of any such abundant and intimate assoc-
iation of fused rock and heated water as would tend to their for-
mation ; for, while it has been clearly shown by M. Fouque and
Michel-Levy, that diabase and similar basic rocks may be artificially
reproduced in the laboratory from a state of simple dry fusion, it is
extremely doubtful whether any extensive intrusive process produced
by natural causes is ever unaccompanied by a greater or less abun-
dance of superheated water as an integral portion of the fused mass.

In the region under description, the granite pegmatites are, as
usual, by far the most abundant, but there are occasional dykes in
which the occurrence of oligoclase and hornblende as the main constitu-
ents would determine their classification with the diorites.

Composition
of pegmatite.

In composition, these pegmatite masses consist essentially of
quartz and the more acid felspars, chiefly orthoclase, oligoclase, albite
and microcline, while muscovite is the prevalent ferro-magnesian con-
stituent, when any is present, and hornblende and biotite are much less
characteristic. The parallel intergrowth of orthoclase and albite
to which the name perthite lias been applied, is an abundant and sonje-
times prevailing felspathic constituent of the pegmatite dykes, especi-
ally in the vicinity of Mattawa. The composition is therefore some-
what variable, but these dykes or vein-like masses are essentially simi-
lar, though somewhat more acid than the normal plutonic rock ox which
they represent the most highly differentiated or final product of con-
solidation. Thus, in those areas where the gneissic rocks contain a sup-
erabundance of basic material, with plagioclase as the predominating
felspathic constituent, the associated pegmatite usually shows a cor res

■AHIOW

ponding

most abi

pegmatil

ponderar

region, is

pegmatit

muscovit

normal p,

ance of h

of the iro

the miner

The pej

to call for

In other d

developme

pegmatite

Claire stat

are usually

some of tl;

by Mr. R.

locality by

com para tivi

an abundan

Erables rap

its most per

acid bands

abundant a

gneisses nea

east of Matt

of the Iarg(

however, a c

The intrus
that the vari
manner due i
disproved, wl
phase or final
lization of cei

*Annual R«
March, 1899, p.

■J

COMPOSITION OF QMISSES.

63 I

ponding increase in relative basicity, oligoclase seemingly being the
most abundant felspar. In areas of hornblende-granite, the associated
pegmatites contain hornblende as the coloured constituent. The pre-
ponderance of the granitite gneisses or hiotite-granite-gneisses in this
region, is represented also by a far g»-eater relative abundance of the
pegmatitic phases of such rocks, while the far greater prevalence of
muscovite, which usually occurs altogether replacing the biotite of the
normal parent plutonic, evidences the presence of the greater abund-
ance of heated water tending to the more or less complete elimination
of the iron present in this bisilicate and the consequent conversion of
the mineral into muscovite.

The pegmatites have not yet been examined sufficiently in detail Accessory
to call for any lengthy mention of their accessory or accidental minerals.
In other districts these masses are especially noted as favouring the
development of many of the more unusual and rare minerals. In a
pegmatite dyke cutting gneissic rocks about a mile north-west of Eau
Claire station, opaque crystals of beryl occur. The crystals secured
are usually of a pale yellowish but sometimes of a bluish colour and
some of them would exceed five pounds in weight. An examination
by Mr. R. A. A. Johnston, of some specimens collected from the same
locality by Mr. C. W. Willimott, showed likewise the presence of the
comparatively rare minerals, xenotime and polycrase. Cyanite, although
an abundant constituent of the granitite-gneisses in the vicinity of Les
Erables rapids and the mouth of Snake Creek on the Ottawa, exhibits
its most perfect crystallographic development in the coarser and more
acid bands which are evidently of pegmatitic origin. Fluorite is also an
abundant and frequent constituent in the pegmatites cutting the
gneisses near the Ottawa in the township of Cameron, about five miles
east of Mattawa. In the necessarily more or less hurried examination
of the large number of these pegmatite masses, there was found,
however, a conspicuous monotony in composition.

The intrusive character of pegmatite is now so generally recognized,

that the various theories, formerly extant, regarding it as in some

manner due to aqueous infiltration and deposition, may be considered as ^ . .
1. 1 , ., , . , . . , Tntrusive in

disproved, while the view that pegmatite constitutes the most acid cliaracter.

phase or final differentiation product attending the progressive crystal-
lization of certain intrusive plutonic rocks has been very clearly and

*Annual Report, Geol. Surv. Can., vol. IX. (N.S.) p. 13 R ; also Am. Jour. Sc,
March, 1899, p. 243 : also Summary Report Geol. Surv. Can., 1898, p. 167.

64 I

NIPISSINO AND TEMISCAMlVa KEOION.

OpinioiiH of
.Messrs. W. ()
C''rosl)y and
M. F. Fulinr.

Forniiition of
lie^fuiatite.

ably set forth by Lehniiinii*, Broggerf, Williams J and others, and all
have given expression to the opinion that water played a most import-
ant role in their formation. Probalily the most satisfactory explana-
which has yet appeared, is that lately issued as the joint production of
Messrs. W. O. Crosby and M. L. Fuller, (^f Boston. S These author.s
recognize " that the most satisfactory explanation of this blending of
the pegmatite with quartz vvina on the one hand, as with the normal
granite (m the other, is to be found in a corresponding blending of
aqueo-igneous fusion with igneo-acjueous solution ; and this dynamic
gradation, it appears to us, can only result from the gradual hydration
of the residual magma during the slow centripetal solidification of a
body of magma and a consequent elimination of water."

Til ihis paper the authors further state that pegmatite should be
regf.ided, " not as a distinct specie.i or family of rocks, but rather as a
possible textural phase of all, or nearly all, the plutonic rocks ; and we
may, in general, say of any plutonic rook, that it may be crypto-crystal-
line, microcrystalliue, macro-crystalline or pegmatitic."

The consensus, therefore, of recent opinion, seems to favour an
intrusive origin for pegmatite, the progressive increase in hydration
of the residual magma being explanatory by a corresponding increase in
acidity of its later crystallization.

The stages represented completely by the occurrences in this region,
show a perfect and practically uninterrupted continuity during the
consolidation of these rocks, from an original condition of hydro-igneous
fufion characteristic of the magma from which the comparatively fine
and even-grained parent plutonic is generally believed to have resulted,
to conditions of aqueous solution which must have obtained in the
viscous mass from which the latest quartzose segregations have solidi-
fied. Such views are in harmony with the known occurrences of most
of the quartzose masses and veins, so frequently present in these Archa'an
rocks, and which have evidently originated by a process closely allied
to that described above, in consequence of the deposition from super-
saturated solutions of highly siliceous material, and are substantially
contemporaneous with the parent plutonic mass with which they are
so intimately associated.

*Ueber die Entsehung der altkrystallinischen Schiefergesteine 1884, p. 24etBeq.

f Die Mineralien der Syenitpeginatitgiinge der siidnorwegisphen Augit und Nephe' ''
syenit I, Theil pi). 21.5-225. Translated by N. N. Evans, Can. Rec. Sc, vol. V
No8. 2 and 3, pp. 33-4(5 and (Jl-71.

JOrigin of the Maryland Pegmatites, XVth Ann. Rep. U. S. Geol. Survey, pp.
675-686.

§Technology Quarterly, vol. IX., No. 4, December, 189G, pp. 326-356.

MKLOW

Thi

as tht

covite

sion ij

of idi

quarts

crysta

ment (

these

occur n

crystal

especia!

seems

materia

stricted

not onlj

partialis

composii

The e

formatio

plutonic

progress

Of receni

holocryst

plutonic

to a porp

pointed o

posed mat

the progr(

The ino
masses, is
striking cf
plutonic ro
of the quai
"olely to la
Liiat It is
between th
t- aiewhat i
presenting
walls, and
is often occu
5

•]

COMPOSITION OF ONEISSES.

65 I

The nge relations of the component minerals are practically the same A^'i- lulatidnM

1 • .1 1 , !• 1 • 1 nil 1 • ,.•! of coIIllHpnfllt

as that in the more usual types or plutonic rocks. Ihus biotite, mus- niiiunilH.
covite, and the more basic felspars, crystallized out in regular succes-
sion in the order mentioned, showing a gradual decrease in perfection
of idiomorphic development. The more acid felspars, and finally the
quartz follow, the latter, especially, showing little or no evidence of
crystal boundaries, occupying the interspaces left by the earlier develop-
ment of the more basic constituents. When drusy cavities exist in
these pegmatites, as well as in the quartzose and more vein-like
occurrences, the silica sometimes exhibits a decided tendency towards
crystalline development. The presence of such unfilled spaces,
especially in the immediate vicinity of such perfect crystal forms,
seems to furnish evidence of the insufficiency of the siliceous
material in solution to fill the spaces, permitting a more or less unre-
stricted development of the remaining quartz. They likewise point,
not only to the extreme acidity of the last remaining portion of the
partially solidified magna, but also to its approximately homogeneous
composition.

The exact depth below the earth's surface necessary for the
formation of these pegmatites and their parent masses of normal
plutonic rocks, as well as the amount of pressure during the
progress of their crystallization, is a mere matter of spe-^ulation.
Of recent years a perfect gradation has been traced from tha typical
holocrystalline structure characteristic of granite, gabbro and other
plutonic rocks, in a vertical distance of a few hundred feet upward, in-
to a porphyritic phase at the surface ; while the pressure required, as
pointed out by Brogger, would be obtained by the presence of superim-
posed material, great enough to prevent the water, separated out by
the progressive crystallization, from escaping freely to the surface.

The most distinctive feature concerning the development of the; e Coarse coxtnie
masses, is their extremely coarse crystalline texture, which is in very I'fKin'itite.
striking contrast to the normal or usual crystallization of the parent
plutonic rock with which they are associated. The resemblance in many
of the quartzose varieties to quartz veins, originally regarded as due
solely to lateral secretion and aqueuus deposition, is so very marked
that it is difficult to see how any hard and fast line can be drawn
between these separate occurrences. Usually in these cases there is a

aewhat indistinct zone-like arrangement of the material, the masses Some quartz
presenting a finer grained felspathic portion in the vicinity of the ^n."titic* m
walls, and showing a continuous transition towards the interior, which orij^in.
is often occup' d by comparatively large allotriomorphic masses of almost

1 H

s n-:

i i'

66 I

NlPISSIXr; AND TEMISCAMING IlEGION.

pegmatite.

Coin])()sii:iop
of i)fgiiiatitt',

pure quartz. Uaually there is a perfect gradation into the parent
plutonic whan this is the inclosing rook-mass, while an undoubted
passage can very frequently be traced into areas of pure quartz, and
occasionally into rather typical or ordinary i[uartz veiixS.

Two phases of In the rt^gion embraced by this report, there are two somewhat
distinct plif.aes of such rocks. The most frequent and abundant is
perhaps represented by the acidic facies of the gneisses constituting
the coarser and more felspathic and quartzose bands. These present
ail the distinguishing characteristi<;s of pegmatite, jilthough occurring in
perfect conformity with the prevailing fc'.i.cion. In composition they
show the usual great preponderance of felsf>ar and quartz, with only
very occasional flakes of biotite, which in many cases hns undergone
notable bleaching owing to the 'elimination of a considet-able pro-
portion of the iron originally present. Such biotite is much paler in
colour, with less marked pleochroism, and shows the brilliant clu'omatic
polarization colours, though p^;i'haps in a less degree, so characteristic
of the lighter' coloured mica. The most frequent and abundant
coloured constituent, however^ is muscovite, which in some cases, at
least, is an original constituent, although a great deal has undoubtedly
resulted from the alteration of the biotite. These pegmatitic bands
very evidently re|iresent the residual and more acid portions of the
magma which liave crystallized iti situ, and may be referred to as
examples of what has been called "sedentary pegmatite." They
usually show a perfect, tliough somewhat rapid, transition into the more
basic bands imiiiediatt;ly adjoining, and are therefore to be regarded
as more strictly contemporaneous than those constituting the second
mode of occurrence. These are masses or apophyses of residual and con-
se(iuently more fully hydiated and acid portions of the magma, which
have invaded and tilled various cracks and fissures occurring in the
gneissic massif or in the neighbouring clastic ''icks. They are usually
present in more or less marked conformity with the foliation of the
gneissic rocks, but very often fill rifts which intersect this at consider-
able angles. Although in the detail of their structural relations, many
of these occurrences are obviously newer than the associated gneisses,
the general examination of the masses throughout the whole area
seems to show that they must be regaided as substantially of the same
age. The process of crystallization was evidently practically continu-
ous, from the first development of the earlier constituents in the still
molten and ^'^scous magma to the filling in of the most minute cracks
and fissures by the remaining quartz, marking the final step in the
complete solidification of the whole masn. Intimately associated geneti-
cally with these pegmatites, are certain veins and even veinlets of quartz.

Sedentary
pegmatite.

Structural
relations.

Relative age.

Metliwl of
formation.

sometin.
the prev
These ar
contact 1
and it se
tions of si
of the nu
so freque

In thoi
present h
position, 1
parallel al
or nuclei c
uents. S
than the r
erable mas
the irrupti
are simply
they merg(
both are sti
to the norti
and Anniff
more or le
scales resul
This foliati
slates on tl
centre of t
end of Ore
glomerate o
but which J
foliated gne
basic mater
ever expose
and microcl
tion of a rat
passes by ir
exposed on
field station
rock is 80 m

lere

g»

magma has

■ARU>«i

]

OOMPOSITION OP GNEISSES.

• 7 I

sometitL containing felspar, which penetrate and anastamose through Origin of some
the prevailing gneisses as well as through the clastic rocks of this district. ^'"'^'
These are especially numerous and M-ell developed along the lines of
contact between the various plutonic masses and the Huronian elastics,
and it seems probable that by far the greater number of these infiltra-
tions of secondary quartz are due to the extravasation and differentiation
of the numerous large masses of these deep-seated irruptives exposed
so frequently throughout this area.

Foliation of

liouiogoneoiis

gniMssos.

Kt'!ati .t" age.

Granite

around

Anninia-

lll'.llllSS

Tjake.

In those portions of the area coloured as Lanrentian, wher^ the rocks
present have solidified from r. magma more or less homogeneous in com-
position, the foliation generally present is seen to consist usually of a
parallel alignment of the biailicate individuals, or, at most, of small nests
or nuclei composed of an aggregate of scales or fragments of such constit-
uents. Such rocks are in many instances of somewhat later generation
than the more evenly foliated gneisses, and frequently contain consid-
erable masses or fragments of these that have been caught up during
the irruption of the former. At other times, such homogeneous masses
are simply more granitoid portions of the prevailing gneiss, into which
they merge both across and along the strike of the foliation, so that
both are strictly contemporaneous with one another. The area of granite
to the north-east of Lake Temagami, especially in the vicinity of Carrying
and Annima-nipissing lakes, has a marked foliated texture, due to the
more or less parallel disposition of aggregates of greenish chlorite
scales resulting from the decomposition of the biotite originally present.
This foliation is more pronounced near the junction with the Huronian
slates on these lakes, gradually fading on passing inwards towards the
centre of the mass. On Lake Teraiscaming, as well as near the south
end of Cross Lake, the Laurentian in contact with the breccia-con-
glomerate of the Huronian is a massive granite, very poor in bisilicates,
but which gradually merges southward into very typical and evenly
foliated gneiss, showing the usual alternating sequence of acidic and
basic material. In the vicinity of Lake Nasbonsing, the rock, where-
ever exposed, is a massive flesh-coloured gneiss, very rich in orthoclase
and microcline, while the foliation is produced liy the parallel disposi-
tion of a rather sparing quantity of hornblende ard garnet. This rock
passes by insensible gradations into the more evenly foliated varieties
exposed on the north sliore of the lake between Nasbonsing and Bon-
fleld stations, although in the vicinity of Bonfield station itself, the
rock is so massive thaL little or no structural details could be traced.

Where greater ln^tarogeneity in the original composition of the Foliation > if
magma has prevailed, the foliation present shows a correspondizig fil!^,!**"

Ijaurentian on
Tcniiscaiiiing
and Cross
Lakes.

(ini'issof Lake
Xaslxjnsiny.

ogt'iieous
composition.

68 I

NIPISSING AND TEMISCAMING REGIOX.

''I;
fill

il . H^

i m

Structural
relations.

Methtid of
formation.

Dynamic
a.^tion.

increase in the perfection of its development, consisting cas it does of
alternating bands of lighter and darker coloured material, representing
numerous varietal forms of rock-types which may be referred respect-
ively to either the acidic or basic gn.ups already mentioned. This
foliation it is which generally characterizes the rocks exposed in the
area covered by the accompanying map-sheets.

The component bands are of variable thickness. Occasionally there
is an exceedingly sharp line of demarcation between the alternating
folia, but as a general rule there is a complete, though somewhat rapid
transition from one to the other. Even in their subordinate arrange-
ment the constituent bands show the same marked tendency towards
parallel arrangement, and a thick bed of prevailing felspathic com-
position will, in cross section, present .short dashes or small patches
of biotite or hornblende all drawn out in one direction ; while, on
the other hand, the more basic portions show a similar definite arrange-
ment of long lenticules of lighter coloured material, in which a relatively
greater amount of felspar or quartz is present. The continuity of
these folia, both large and small, is broken at frequent intervals, some-
times abruptly, but usually by a gradual thinning out in either direction.
Frequently, before such interruption takes place, bands of essentially
similar composition may be formed immediately above or below, which
in tui*n pinch out in both directions to be again replaced by others.
This irregularity in horizontal arrangement is equally true of their
downward or vertical extension, so that the whole section, of even a
small area of any such rock-exposures, presents an exceedingly compli-
cated arrangement of lighter and daiker material of greatly varying
acidity and basicity. It is quite evident from their macroscopic arrange-
ment, that their formation was attended with an extremely gradual
diminution of temperature, for the frequent absence of sharp lines of
demarcation between these bands of widely different composition, seems
to point to the re-absorption by the later and more acid portions of the
magma of the first formed or faster cooling basic portions, perhaps many
limes repeated before the final consolidation of the whole mass.

In many places, the dark bands evidence the action of extensive
crushing and crumpling, showing that great movements have taken
place in the whole series. These movements were doubtless approxi-
mately synchronous, and closely connected with tlie invasion and
cooling of the more .acid portions of the magma. The most curious
and coniplicated structures are thus often produced, this complexity
being enhanced by the frequent dislocation, accompanied sometimes
by considerable separation and displacement, of those portions which

BARLOW

COMPOSITION OF GNEISSES.

69 I

evidently existed originally in unbroken continuity. Such intricate
structures are, however, usually extremely local in their development,
the gneiss elsewhere in the vicinity often showing little or no sign of
extreme disturbance. Although, as a general rule, the direction of this
foliation shows a marked uniformity over large areas, there is a con-
siderable diversity in arrangement in this regard, as indicated on the
accompanying maps,

A careful correlation of the many observations made, shows clearly Mode of
that these gneissic rocks occui- for the most part in the form of large "'^''"''''snce.
rudely oval or concentric masses whose longer axes have in general a
direction according with the prevailing strike of the foliation. Fre-
quently such large ovoid masses present quaquaversal dips, which in
cross-section simulates the ordinary anticlinal arch. About a mile east
of Mattawa station, the Canadian Pacific Railway cuts through a small Structural
dome of these gneissic rocks, composed of beautifully sharp alternating '^''' "'^'^'^*
felspathic, micaceous and quartzose bands, showing a remarkably per-
fect example of very pronounced differentiation. The section as pre-
sented on either side of the railway track, presents a marked resem-
blance to a low anticlinal dome. Plate III. The truly igneous
character of the composing rocks, however, v^ould not permit of such
an interpretation. In size these ovoid masses vary greatly, some of
the curvings belonging to ellipsoids many miles in diameter while
others are a mile or less in diameter.

As a rule the folia or lamince have a prevailing dip to the south-east
or south, which is singularly uniform over large areas. This inclina- Dip.
tion is generally rather steep, usually considerably over 45°, while,
frequently, as in many places along the shores of Lake Temiscaming,
the foliation is almost, if not quite, vertical. On Seven League
Lake and southwards to Mattawa, as well as westwards to Tomiko
Lake, the bands frequently succeed one another in almost hori-
zontal succession, the dip, if any, being generally southwards at a
low angle. Even in this area, however, there are frequent exceptions
to this rule, and the rocks often show a rapid change in this prevailing
horizontality as though the bands had been subjected to frequent
disturbances and dislocation during the progress of their formation.
Thus in the vicinity of North Bay and the northern portion of Lake
Nipisiing, the gneisses often approach a vertical attitude, while on
the southern shores in the vicinity of French River, similar rocks
are nearly horizontal.

'i i;

70 I

Work by

iMesHi'H.
Kerrier uirI
Barlow.

Ohject of
studies.

Classificatiiiii

of glU'isSft^.

Princi|)li' of
classificati(jn.

NIPISSINO AND XEMISCAMINO REGION.

PBTKOGRAPHY OF THE LAUBENTIAN.

The petrographical work done in connection wich the present report
was carried out with the co-operation of Mr. W. F. Ferrier, Litliologist
to the Geological Survey, to whom credit must be given for many of
the results obtained.

The writer and Mr. Ferrier worked in conjunction on the problems
involved and with so free an interchange of ideas throughout, that no
attempt will be here made to separate the examinations, more than to
mention that many of the more critical specimens were made the
subject of special study by Mr. Ferrier.

The main object of these detailed studies has been, not only to obtain
more accurate information with regard to the composition and minute
structures of the various rocks, but also to gain an increased know-
ledge of their origin and the relationship existing between the alter-
nating bands of relatively greater or less basicity.

Incidentally, a table has been prepared, showing a classification of
these old crystalline rocks, displaying not only their composition, but
also their close affiliation with one another. This table may recom-
mend itself to petrographers, as it has done to the authors, and it is
hoped may be found of material use in future work undertaken in
areas of similar Archaean gneissic rocks.

Much microscopical work has also been accomplished in connection
with a series of specimens taken as illustralive of the various contact
phenomena exhibited along the line of junction between the Lauren-
tian and Huronian. This has enabled a more accurate interpretation
and description of the various facts having reference to the relative
ages of th^-^e two series of rocks. Field-work, no matter how careful
or extended, in areas characterized by the presence of Archtean strata,
must of necessity lose much of its value if unaccompanied by concurrent
petrographies) 1 studies. In the present instance, the results have been
adduced, not only from a critical and extensive examination of the
numerous rock-exposures in the field, but also by a careful correlation
of the facts thus ascertained with those acquired in the petrographical
laboratory.

Classification.

Any system of classification applied to sucli a series of foliatefl rocks
must, necessarily, in some respects, be unsatisfactory ; but a grouping
together according to their mineralogical composition seems on the

BARIOW. I

whole
knowlf

As a
petrogi
allied i
plutoni
might 1
sometiu
ance or

It mi
arbifcrar
to a cer

excludir
petrogra
examine
referred.

Xo ati
collected
selected i

As pre
two greai
dominant
Biotite is
first divis

The fir;
on the
Arranged
collectiop.

vj-nui

epidote.

2. Gnei

3. Gnei

4. Gneii

5. Gneis
biotite.

6. Gneif

7. Gneis

Tlie rela
be seen by

i I

■]

PETROGRAPHY OF THE LAURENTIAN.

71 I

ation.

whole to be the best that can be cadopted in the present state of our
knowledge.

As already stated, however, there cau be no doubt that all of the
petrographical types represented in the gneisses from this region are
allied iu their chemical composition and mineral constituents to such
plutonic igneous rocks as granite, syenite, diorite, gabbro, etc., but, as
might be expected, there is a passage from one rock-type to anotlier,
sometimes gradual, sometimes very abrupt, according to the abund-
ance or scarcity of certain minerals.

It must be borne in mind that the classification here adopted is an 9''^*"^**^^.

. » , classificati

arbitrary one, based on the mineralogical composition of the rocks, and

to a certain extent on variations in their structure, the object bein;.;,

excluding theoretical considerations, to establish certain well defined

petrographical types that have been found to be constant in the area

examined, and to which specimens from other districts may be

referred.

No attempt has been made to examine minutely all the specimens
collected, but good examples of the more prevalent types have been
selected and described in detail.

As previously stated, the gneisses of the region may be placed in pnoissesdlvis-
two great divisions, the acidic, characterized by orthoclase as the pre- great classes.
dominant felspar, and the basic, by the predominance of plagioclase.
Biotite is by far the most abundant ferro-magnesian constituent of the
first division, and hornblende of the second.

The first division may be subdivided into seven groups, dependent Acidic
on the presence of one or other of the coloured constituents. divid^Hnto
Arranged, approximately, according to frequency of occurrence in the '**^^'p» groups.
coliectiot\ tlijy are as follows ; —

i. Criuisses characterized by the presence of biotite and primary
epidote.

2. Gneisses in which biotite alone is present.

3. Gneisses in which both biotite and rauscovite occur.

4. Gneisses in which hornblende accompanies the micas.

5. Gneisses in which cyanite, graphite, garnet, etc., accompany the
biotite.

6. Gneisses in which hornblende alone is present.

7. Gneisses in which muscovite alone is present.

The relationship of these rocks to their analogous massive types may
be seen by reference to the accompanying table.

I '

k' r

Two varieties
of l)asic
gneisses.

No arbitrary
line possible.

Absence of
augite.

'2 I

NIPISSING AND TEMISCAMING REGION.

Of the second division, the basic, or hornblende gneisses, two varie-
ties may sometimes be distinguished, first, those which represent seg-
gregated bands of the more basic material of the original granitic
magma, and secondly, those which are undoubted basic eruptives
folded-in with the more acidic gneisses.

It is not always possible to make this distinction, but examples of
each of these two varieties have been observed.

Classified according to their mineralogical composition they naturally
must be placed close to each other.

Amongst the first, whilst certain names have been applied to individ-
ual specimens, it is manifest that no hard and fast lines can be drawn
in the field. For instance, a band of which one portion would have
the mineralogical composition and characters of a quartz-mica-diorite
may pass insensibly into material having all the characters of a horn-
blende-granitite, according as the plagioclase diminished and monocli-
nic felspar increased in quantity.

One remarkable fact in connection with these basic bands, is the
great scarcity in them of augite, none of the hornblende containing
cores of that mineral, or affording any direct evidence of having
originated from it.

In the Laurentian area lying to the north of the Island of Montreal
recently described by Dr. Adams,* on the contrary, the basic bands in
the gneiss appear to consist largely of pyroxene rocks.

/. — 2'he Granite-gneisses.

Orthoclase
gneiss.

Composition.

In colour these rocks range from a light-gray to a decided red. The
red rocks represent what has usually been called by the older writers
on the Archaean, the "red orthoclase gneiss," but we find in the field
every gradation from the gray to the red gneiss, the one passing im-
perceptibly into the other in many localities, and the microscopical
examination has failed to detect any essential point of difference between
these two varieties.

The red gneisses contain a large quantity of hydrous iron-oxides
distributed through them, to which the coloration is due, and they

* Annual Report, Geol. Surv. Can., vol. VIII. (N.S.), Part j,, 1890.

BARLOA

PETROGRAPHY OF THE LAURENTIAX.

73 I

also appear to have a larger proportion of microcline than the gray
ones. Plagioclase was not observed to exist in any greater quantity
in the gray varieties than in the red ones.

Many of the more altered mica-gneisses have assumed a dark-green Chloritization
colour, owing to the chloritization of the biotite, but microscopic ex- ' J"'*''"-
amination shows that they may be included in the same class as the
typical unaltered ones.

These chioritized raica-gneisses have been freciuently, though erron
eously, sp>)ken of as hornblende-gneisses by the earlier geologica'
observers in this region, who were misled by their colour, and had not
the advantages afibrded by microscopical examination of the rocks. A
remarkable feature of these gneisses is their comparative freedom from
iron ores.

When pyrite occurs, it is almost always associated with large clove-
brown sphenes.

In the case of the micaceous gneisses, i.e., those in which biotite Scarcity of
alone, or biotite and muscovite together constitute the predominating liornblende.
ferro-magnesian constituents, hornblende was observed in only two
instances, and then in minute quantities.

The almost total absence of augite from these rocks is to be parti-
cularly noted. Even in the basic hornblende-gneisses of the region,
this mineral is very rarely, if ever, to be found.

A. Biotite muscovite gneisses — [Granite-gneiss). — The rocks grouped structure,
together under this heading are, like the other gneisses, holocrystal-

line and granitic in their structure. Both biotite and muscovite are
present as the chief, and in fact almost the only coloured constituents.
These two micas occur intergrown with each other in aggregates of Composition,
broad fresh plates. The specimens representing this rock-type a"e,
apparently, not very numerous in the collection. Those examined are
remarkably free from epidote, iron ore and titanite.

Orthoclase and microcline are the predominating felspars, and
granophyric intergrowth of the quartz and felspar is a common
feature.

B. Muscovite-granite-gneiss— {Pegmatite in part). — The rocks thus
designated and classified, are of comparatively rare occurrence as strictly
integral portions of the gneissic complex, and where present constitute
the latest secretions from the original magma.

74 I

NIPI8SING AND TEMISCAMING REGION.

ComiKDHitioii
of muHcovite-
granite-gneiss.

I Iff:

II!

I I

(Iranititi^

gneisses.

Biotite-
epidote-
giieisa.

Biotite-gneiss.

In reality they represent interfoliated bands of pegmatite, although
of much finer texture than the rock to which that name is usually
applied. In colour they are wliite, light-gray, or pale-pink,
presenting glistening or pearly cleavage planes. Under the micro-
scope they present the usual interlocking holocrystalline aggregate of
quartz, orthoclase, plagioclase (oligoclase) and microcline, with a
smaller amount of sericite (hydrous muscovite) arranged in long drawn-
out scales, and plates which traverse the rock in curving and
approximately parallel bands. A small quantity of epidote find
zoisite in crystals and grains, some of which may be primary-, is
associated with small scales of sericite, the latter, at least, being one
of the products of the incipient decomposition of the felspathic con-
stituents. Occasional small flakes or scales of a much bleached
biotite occur, some of which form a parallel intergrowth with the
muscovite. The specimens examined have undergone extensive defor-
mation, as a result of pressure subsequent to the cooling of the rock,
and both felspar and quartz have suffered a somewhat marked granu-
lation, while the surviving individuals of both the.se minerals exhibit
wavy extinction rather perfectly. Some of the muscovite is
doubtless of primary formation, although some has evidently resulted
from the shearing of the felspar.

C. Biotite-granite-gneissfis — (Gramfitft-gneisses). Var. («) Biotite-
epidote-gneiss. — The combination of biotite and epidote as the prin-
cipal coloured constituents, forms a well defined rock-type which has
been found to be remarkably constant over large and widely separated
areas, and is the one which is represented by the largest number of
specimens.

These rocks are undoubtedly of irruptive origin, and are, in fact,
foliated granitites, thoroughly holocrystalline and granitoid, varying
from coarsely to finely crystalline ; the constituent minerals being, a.s
a rule, equally developed on all sides.

Var. (6) Biotite-gneiss. These are foliated, holocrystalline,
granitic rocks in which biotite alone, or accompanied by very trifling
(juantities of secondary epidote, is the ferro-raagnesian constituent.

Biotite-
cyanite-
giieiss.

In the specimens of this type of rock which have been examined,
the mineral does not occur, as a general rule, in aggregates of broad
plates, but in isolated independent ones, which have an approximately
pai'allel arrangement, determining the foliation of the mass.

Var. (c) Biotite-cyanite-gneiss. This gneiss, though somewhat re-
markable in its mineral composition, in that it contains cyanite, garnet.

lighter a

BARLOW.

]

PETROORAPHY OF THE LAURENTIAN.

I -J I

and graphite in addition to the biotite which chiefly characterizes it,
does not present any evidence whatever, either in its inicroscopicfil
structure or its field relations, of any other than an irruptive origin.

It is a perfectly fresh, holocrystalline, foliated granitic rock, and
possesses in its structure no features which would at all suggest re-
crystallization. It seems to be a peculiar local phase of the prevalent
biotite-gneisses of the region, differing in no way from them as regards
origin.

A somewhat similar gneiss from near Wahnapitae station, in the Uescription of
Sudbury district, has recently been petrographically described by Dr. ^J!''',?** ^^ ^^^
T. L. Walker,* who, however, says little regarding its microscopical
character and field relations, beyond assigning it to the Laurentian,
and stating that he regards it as a " true gneiss " and not a crushed
granite.

Var. (d) Hornblende-granititegneiss. — The rock thus classified Hornblende-
differs but little in microscopical character from the ordinary mica- ^'r'u.ntite-
ceous form of the granitites, although usually darker in colour and
more basic in appearance. It sliows a transition ou the one hand into
granitite containing biotite alone as the coloured constituent, which
is the prevailing type of these gneissic rocks, and on the other, into
hornblendegranitegneiss, which latter facies is of rather rare occur-
rence throughout the district. In all previous descriptions the honi-
blende-granite-gneiss has been reported as the variety most commonly
present in the I^aurentian, the mistake having undoubtedly arisen from
tht Vequent chloritization of the biotite originally present in the pre-
valent granitite, the individuals showing the more advanced stages <if
decomposition bearing a marked macroscopical resemblance to those of
the ordinary green trichroic hornblende usually noticed in these Arcli-
ffian rocks. The rock presents the usual reddish or grayish colours,
and, where highly differentiated, exhibits the usual interfoliation of
lighter and darker coloured bands, although the lenticular areas or
patches of the former are relatively less abundant and of smaller extent
than those of darker hue. The structure of the rock is holocrystalline ; Composition
it is composed of quartz, orthoclase, plagioclase, microcline, biotite and ''"'^' structure
hornblende as the chief or essential constituents, together with a much
smaller quantity of ilmenite (in part altered to leucoxene) magnetite 1
sphene, epidote, apatite and zii'con, as accessory or accidental constitu-
ents ; while chlorite, calcite, and sericite usually occur in more or le-s
abundance as secondary products of decomposition. Hornblende is

il !'

*Cieological and Petrographical Studies of the Sudbury Nickel District.
Journ. Geol. Soc, vol. LIII., p. 42, 1897.

Quart.

(I ;■

t-^K

76 I

NIPISSINf! AND TEMISCAMING UECilON.

I* t

the inost abundant ferro-magnesian mineral in the more basic portions,
while biotite predominates in the lighter coloured patches. The rock
presents no unusual features as regards crush phenomena, the compon-
ent individuuls of felspar and quartz usually showing little evidence
of having been subjected to any very considerable pressure subsequent
to consolidation.

Hornbkndf- D. IIoriMende-granite gneisses. — This facies of rock seems to be of
gram e-gnems. j,.^j_jjgj. limited and rare occurrence in the district under description,
and the specimens from which the thin sections were prepared for pur-
poses of study were obtained in close proximity to masses of basic pyro-
xenic or hornblondic material. Their composition and association has
suggested that the rock may represent a connningling or transference
of material through fusion of the substance of both rocks. The rocks
thus classified resemble very closely the hornblende-granites, with
which they are intimately related. The most common of the essential
constituents are quartz, orthoclase, microcline, plagioclase and horn-
blende, with sphene, apatite, iron ore, zircon, epidote and garnet as
accessory minerals.

The colour varies greatly, depending largely on the composition, the
more basic portions being dark -greenish to almost black, while the aci-
dic bauds are grayish or reddish.

Certain of the more massive and homogeneous varieties of these
rocks have a distinct Hesh-red colour, with a greenish tinge given by
the prevalence of the hornblende.

In common with the rest of the gneisses, these rocks have been sub-
jected to pressure of varying intensity, resulting in the granulation of
the quartz and felspar.

//. — Syenite Gneisses.

Syenite-gneiss These do not appear to have many representatives amonj^st the
rocks of the region. Those observed correspond to the mica-syenites of
the massive plutonic igneous rocks and may be termed : —

Mica-syenite-gneiss. — This is a holocrystalline, foliated rock char-
acterized by the almost total absence of quartz, and the presence of
biotite as the principal ferro-magnesian constituent.

Orthoclase is the prevailing felspar in the typical examples, but in
the one specimen which was examined a plagioclase (oligoclase or albite)
was found to constitute nearly 50 per cent of the felspar present in the
section.

\mmy

BADLOW.

]

PETROORAPHY OF THK LAURENTIAN.

77 I

These rocks are unduubtodly the foliated equivalents of the massive
mica-syenites, wliioli, as is well known, frequently contain a consider
able quantity of albite in addition to the ortliociase and biotite.

///. — Diorite Gneisses.

Var. (a) Qaai'tz-mica diorite-gnflins. — Macroscopically, this rock DidritcmuiMH
is of a dark-gray, almost black colour, very evenly foliated, and
presenting; brightly glistrMiing cleavage surfaces. Sometimes very nar-
row interfoliated bands are more acid in composition, and have a red-
dish or grayish tinge owing to the presence of a considerable (juantity
of felspar and quartz, more or less stained by hydrous oxide of iion.

Both in the field and under the nucroacope, these are seen to merge
gradually into the more basic varieties of the granite-gneisses, from
which they differ chicf.y i.i that the ortliociase is replaced by plagio-
clase as the predominating felspathic constituent, while hornblende,
instead of biotite, is present as the principal ferro-magnesian unneral.
Biotite, as well as quartz, is invariably present, the latter mineral ( omposition
occurring in considerable quantity, even in the most basic phases of the mica-diorit.'
rock,while both these minerals are always abundant enough to character- ^'"•'i'*'''
ize it. The constituent minerals are essentially identical with
those noticed as present in the more basic types of granite gneiss, dif-
fering only in the order of their relative abundance and iuiportan<e.
The coloured constituents, such as hornblende, biotite and sphene,
make up the greater part of the rock, which is relatively much poorer
in felspar and quartz, the most important and abundant minerals
in the granite-gneisses. The essential constituents usually noticed are
plagioclase, orthoclase, quartz, hornblende and biotite. Microcline is
very often present in subordinate amount. Primary epidote, in very
sharp idiomorphic crystals, embedded chiefly in unaltered biotite, and
sometimes penetrated by wedge-like crystals of sphene or titanite, was
frequently noticed. Of the accessory minerals, sphene, apatite and zir-
con are almost invariably present, while pyrite. magnetite, limonite,
epidote and allanite likewise sometimes occur. These basic bands are
undoubtedly integral portions of the same magma from which the more
usual or prevailing granite-gneiss has solidified.

Va7\ (b) Dioritic Gneiss : Amphibolitc. — It has been thought advis- Ampbibolite.
able for the purposes of distinction to use this term " dioritic gneiss,'' not
as implying any difference in origin, but simply denoting that che rock
thus classified does not form an integral or higldy difleicntiated por-
tion of the same magma from which the ordinary gneisses have solidi-
fied. It frequently occurs interfoliated, and often in dyke-like forms,

78 I

NIPIS81N0 AND TEMISCAMING REGION.

Minerals pre-
seut in the
gneisses.

evidently representing portions of some pre-existing basic irruptive
which has undergone excessive crushing, and consequent recrystalliza-
tion, as a result of the subsecjuent intrusion of the associated gneissic
rocks classified as Laurentian. Macroscopically, these rocks are fine-
fjrained, very dark greenish-gray (almost black) in colour, with distinct
foliation and schistosity. When broken, the fresh surfaces show-
brightly glistening crystals, and plates of hornblende and mica. The
rock examined is composed chiefly of compact green trichroic horn-
blende and plagioclase. As is often the case with rocks which have
undergone similar extensive recrystallization, the triclinic felspar pre-
sent is very clear and glassy, showing a frequent and marked absence
of the twinning or pressure lamelhe. When these are present, how-
over, the extinction-angles shown are those characteristic of labra-
dorite, while some of the unstriatod grains may possibly represent
urthoclaso. The quartz present is proportionately very subordinate in
([uantity, and is often with difficulty distinguishable from the clear
and sharply extinguishing felspar. The biotite present occurs in inti-
mate association with the hornblende, sometimes forming parallel
intergrowths with this mineral; garnet and ilmenite, the latter
mineral often surrounded by sphene, are likewise present. In several
instances, the same rock was traced directly and continuously into
larger areas of practically unaltered gabbroic or diabasic material, of
distinctly earlier genesis than the gneiss in which they are embedded.

Minerals of tJie Gneissic Mocks.

The minerals observed in the acidic and basic gneissic rocks are the
following : —

Quartz

Orthoclase

Microcline

Plagioclase

Biotite

Hornblende

Epidote

Muscos'ite

Chlorite

Pyrite

Calcite

Sericite

Apatite

Titanite

Zircon

Garnet

Magnetite

Haematite

Ilmenite

Leucoxene

Limonite

Zoisite

Talc

Tourmaline

Allanite

Rutile

Cyanite

Graphite

Fibrolite

Augite

Of these the quartz, orthoclase, plagioclase, biotite, hornblende,
epidote and muscovite may be regai'ded as essential, and the remainder
either accessory or secondary constituents.

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•]

PETROGRAPHY OP THE LAURENTIAN.

79 I

Quartz. — This is, in general, a very abundant mineral in the Quartz.
gneisoBS of the district. Only in a few cases were granitic specimens
observed in which the absence of quartz would lead to their being
grouped v/ith the syenites. It enters largely into the composition of
the basic rocks, allying them to the quartz-diorites and quartz-niica-
diorites. In its general character it does not differ from the ordinary
granitic variety, but is, of course, much crushed, stretched and granul-
ated in those gneisses which have been subjected to intense dynamic
action.

It appears to fill in the spaces between the felspars of the rock, and
consequently, to have crystallized out of the magt f. afrer they were
formed. This is especially noticeable in many of the basic or dioritic
gneisses. Distinct crystals of quartz have not been observed in the
rocks examined, the mineral occurring in the form of irregular grains.

The quartz grains, as usual, always exhibit the efiFects of dynamic
action in a much more marked degree than do the felspars. A
granophyric intergrowth with felspar is of very common occurrence.
Inclusions are frequent. Sometimes the quartz occurs in grains
scattered through hornblende, the individual grains having no regular
arrangement or orientation with respect to one another or to their
host. Such a structure has been named ' poikilitic " by the late Dr.
George ET. Williams.*

Orfhoclase. — This is the most abundant of the felspars which occur Ortlioclase.
in these rocks. It usually forms irregular grains interlocked with the
other felspars and quartz, although in a few instances porphyritic indi-
viduals occur, which are sometimes twinned. It is seldom quite clear
and fresh-looking, but usually >:' -'^ id in appearance, and more or less
filled with little scales of serlcite avA granules and crystals of epidote
and zoisite, the products of iti r^.ecomposition.

In those specimens representing rocks which have evidently been
subjected to intense dynamic action, the orthoclaso shows a marked
tendency to pass into microcline. Inclusions of the other minerals
present in the rock are of frequent occurrence, and intergrowths with
triclinic felspars were also noted. It is often stained with hydrous
oxides of iron, giving brownish or reddish tints to the rock. In com-
mon with the other felspars, it has escaped to a large extent the results
of dynamic action, rocks in which the quartz has been completely
granulated frequently preserving large grains of the felspars which

*0n the Use of the Terms Poikilitic and Micropoikilitic in Petrography;
Journal of Geology, vol. I, No. 2, jip. 176-170.

jss^acT

Mici'ocline.

i >i

Origin (if
niicrocline.

80 I

NIPISSING AND TEMISCAMING R TO'-

show only a few criicks and a more or less pronounced undulatory
extinction.

Microdine. — This is a very abundant constituent of the granitic
gneisses, especially of those which have been greatly crushed and
granulated. Teall has recently announced that the result of his inves-
tigations of the niicrocline in the older Deeside (Cairnshee) granite of
the Highlands of Scotland "lend no support to the view that micro-
dine may be developed from orthoclase by dynamic or any other action,
but are in accordance with the theory of Michel Levy and Mallard,
that orthoclase is niicrocline in which the polysynthetic twinning is on
a sub-microscopical scale."

The constant relationship which exists between the quantity of
microcline in a given rock and the degree of pressure to which the rock
has been subjected, as brought out by microscopic examination, is of
too marked a character to be ignored, and instances may frequently be
observed, where, when a large individual of orthoclase has been
peripherally granulated, the fragments detached from the parent
individual show to perfection the typical cross-hatching of microcline,
whilst the centre is quite free from striations and exhibits the ordi-
nary characters of orthoclase. There is not, in such instances, a grad-
ual transition from ot.e structure to the other, the cross-hatching in
the detached bit of granulated material next to the parent individual
terminating as abruptly against the fractures which separate them
from it as do the strije induced by pressure in a plagioclase individual,
against cracks traversing the crystal. Where evidences of pressure
are unmistakably present, but fracturing has not actuall}'^ taken place,
the gradation may be seen from the normal orthoclase, through a
"moire structure" to the typical cross-hatching. Plate IV, Figs. 2 it 3.

Thus, whether microcline and orthoclase be identical or dimorphous
(a question which cannot be discussed here) the scarcity of the former
in unaltered rocks, and its marked abundance in those which have been
subjected to pressure, together with the peculiar manner in which it
has been observed to occur in individual instances mentioned above,
.seems to prove rather conclusively that microcline structure at least can
be, and is, produced in the felspar now known as orthoclase and not show-
ing that structure, as the result of pressure. It seems, too, reasonable
to suppose that, if orthoclase be microcline with a sub-microscopic
twinned structure, we should find various gradation.'^ in the same section
from the microscopically invisible structure, through exceedingly fine
striation, to the distinctly visible, and sometimes quite coarse structure,
characterizing; what we call microcline.

BARLOW. 1

Inst(
is subj(
ogous t(
grain oi
evidentl
structur
many of
theory tl
to the cc
d re-arra
Cases
included
regarded
luonoclini

Plagioc
tolerably
-Lake, com
chemical
^•■f tin":, ion
eicner an c

As a gei
with the bi
diorite-gne
a labradori
pressure in

Alteratic

tization of t

sericite. P

In some (

the metamo

clear and "l

probably p

tingui.sh bet

Bintitc-
uent of the
into the coir
in two formf
smaller pJatt

Crystals w
■^rechanical
show the gen

BARLOW

]

PETROGRAPHY OP THE LAURENTIAN.

81 I

Instead of this we find that, when a crystal which we call orthoclase
is subjected to pressure, a peculiar wavy structure appears in it, anal-
ogous to the strain shadows of quartz as seen in the thin section ; the
grain or crystal, when carefully examined under the microscope, being
evidently under strain and undergoing deiormation. This wavy
structure gradually mei'ges into the typical cross-hatched one. In fact,
many of the arguments advanced, and facts cited in favour of the
theory thatmicrocline and orthoclase are identical, seem to point strongly
to the conclusion that this is not the case, but that niicrocline represents
a re-arrangement of the orthoclase molecule induced by pressure.

Cases where areas of felspar with typical microcline structure occur,
included in unaltered and uncrushed orthoclase individuals, may be
regarded as analogous to intcrgrowths of the ordinary triclinic and
monoclinic felspars.

Plagioctase. — In the granitic and syenitic gneisses, plagioclase is ,,, ■ .
tolerably abundant, in the case of the mica-syenite-gneiss from Cross
Lake, constituting nearly one-half of the felspar present. No direct
ch"'nical determinations have been made, but when the angles of
^ :<tiu ' ion have been measured, these indicate that the felspar is
eitner an oligoclase or an andesite.

As a general rule, the proportion of the plagioclase present increases
with the basicity of the rock, and it, of course, predominates in the
diorite-gneisses of the region. In these rocks it is, apparently, chiefly
a labradorite. It is usually well twinned, this twinning being due to
pressure in many cases.

Alteration to calcite was frecjuently observed, also typical saussuri-
tization of the more basic varieties, with formation of zoisite, epidote and
sericite. Poikilitic and micropoikilitic structures are sometimes seen.

In some of the basic gneisses which may possibly have resulted from
the metamorphosis of a basic irruptive, the felspar is fre(inently very
clear and glassy, with numerous unstriated grains which are, however,
probably plagioclase. It is somewhat diflicult, in such cases, to dis-
tinguish between the glassy felspar and the quartz.

Biotitc. — This is by far the most abundant ferro-magnesian constit-
uent of the granitic and syenitic gneisses, and also enters quite freely Hiotit<'
into the composition of the basic varieties. The primary biotite occurs
in two forms, as large, broad plates aggregated together, and as isolated
smaller plates, having a general parallel arrangement in the rock.

Crystals with perfect crystallograpliic boundaries were not observed.
Mechanical deformations of the plates are well seen in the rocks which
show the general effects of dynamic action.
G

Hornblende.

Absorption.

NIPISSING AND TKMI8CAMIN0 REGION.

In most instances, it is remarkably fresh and is intimately associated
with epidote, large, fresh, isolated crystals of which are frequently
inclosed in the unaltered biotite. In colour it is usually a deep
reddish-brown, in some cases inclining to a copper-red, and is very
gtrongly pleochroic, from pale straw-yellow to a deep reddish-brown.
When more or less altered t' chlorite it assumes various tints of green.

Occasionally, in the hornblende-granite-gneisses and diorite-gneisses,
it is intimatelj' associated with tne hornblende. In those rocks which
contain both micas, the biotite and muscovite occur intergrown with
each other, the plates of each variety being sharply defined.

Frequently, however, by a leaching-out process, the iron has been
so far removed from the biotite a& * cause it to assume a very light
colour, indeed in some sections it is difficult to determine whether
certain individuals are to be regarded as bleached biotite or as original
muscovite.

In addition to the biotite which is of undoubted primary origin,
little scales of secondary biotite may often be observed developed along
shear planes in certain of the greatly crushed and stretched gneisses.
The biotite holds numerous inclusions of apatite, zircon, etc., which
are commonly surrounded by dark, pleochroic halos.

Hornblende. — This appears to be a comparatively rare mineral in
those granitic and syenitic gneisses which have l)een examined from
this region. In two instances it is tolerably abundant, but in most
cases where it has been observed, only one or two minute grains could
be detected in a single thin section of the rock.

In the basic or dioritic gneisses it is of course a very abundant
mineral. In these rocks it occurs as the compact variety chiefly
actinolitic forms being rare. It forms, as a general rule, rather irregular
individuals aggregated together, although occasionally some may be
seen having well defined crystallographic boundaries

It possesses good cleavago and is very strongly pleochroic. The ab
sorption is usually f >■ 6 > a generally a greenish yellow ft =dark
yellowish-green, and r = deep bluish-green. Twinning is a common
feature of the mineral.

The hornblende is always intimately associated with the biotite and
epidote when these latter minerals are present in the rock. In several
instances the extinction angle was measured and found to vary from
\1\° to 19°.

Inclusions of felspar, quartz, zircon, apatite, titanite, etc., are very
common and are frequently arranged in such a manner as to give to

•AKLOW

]

the horn
Fig. 1. .
zircon art
ation to
by the de

No inst)

nor any di

the formei

from the fi

the exteric

Ejudote.-

the coloun

largely intc

addition to

duct, we ha

ber of cases

The manr

defined outli

which have

of no reasonj

the accompai

clearly. Th<

pleochroic, ai

tion colours,

exhibit bluisl

both in crystf

stated, very s

The corrosi
Yukon River,
crystal secticr
Good cleavage
them being a)

Twins are o

cores of a p]ec

but no thorou|

Nondescr- )t

of epidote we;

epidote, freque

associated with

*Cau. Rec, S
Can., vol. III. (]v

PETROGRAPHY OF THE LAURENTIAN.

83 I

the hornblende-gneias a typical micropoikilitic structure. Plate II.,
Fig. 1. As in the case of the biotite, the inclusions of apatite and
zircon are often sunounded by well defined pleochroic halos. Alter-
ation to chloritic and epidotic material was observed, accompanied
by the deposition of carbonates.

.No instances of augite cores occurring in the hornblende were noticed'
nor any direct evidence of the latter mineral having originated from
the former ; although in some few instances this might be suspected,
from the fact, that the interior of the crystal is f a paler colour than
the exterior portion.

Epidote. — Next to the biotite, this is by far the most abundant of Epidoie.
the coloured constituents of the granitic gneisses, and it also enters
largely into the composition of the more basic hornblendic ones. In
addition to the ordinary occurrence of the epidote as an alteration pro-
duct, we have also the strongest evidence that it exists in a large num-
ber of cases as an original and important constituent of the rock mass.

The manner in which the perfectly fresh crystals, possessing sharply
defined outlines, occur inclosed by wholly unaltered biotite in rocks
which have been subjected to only a slight degree of pressure, admits
of no reasonable doubt as to their primary nature. An inspection of
the accompanying plate, (Plate II., Fig. 2) will bring this point out very
clearly. The mineral is usually of a bright yellow colour, very strongly
pleochroic, and possessing the usual high relief and brilliant polarizs!
tion colours, except in sections parallel to the orthopinacoid, whicli
exhibit bluish and yellowish tints between crossed nicols. It occurs
both in crystals and irregular gi-ains, the former often having, as already
stated, very sharply defined outlines.

The corrosion phenomena noted by Dr. Adams, in epidote from the Corrosion
Yukon River,* are shown to perfection in some of the individuals. The
crystal sections are usually bounded by the prism planes M, r, and T.
Good cleavages were observed parallel to M and T, the angle between
them being about 115°.

Twins are of common occurrence. The crystals occasionally contain
cores of a pleochroic brownish sub.stance which is probably allanite,
but no thoroughly typical examples of that mineral were detected.

Nondescr' >t cores, which may represent augite, surrounded by rims
of epidote were occasionally seen in the thin sections. Secondary
epidote, frequently occurs in the groundmass of the more altered rocks,
associated with chlorite, as the result of the mutual reaction of the

*Cau. Rec. Sc. vol. IV., pp. 344-358, 1890-91, aim) Annual Report Geol. Surv.
Can., vol. III. (N.S.), Part I, ApiJendix V (N.S.). p. 237 u., 1887-88.

phenomena

' -t:.

84 I

NU'ISSING AND TEMISCAMING REGION.

MRLOW.

felspars and bisilicates. It also forms small crystals and granules in
the decomposing felspars, together with zoisite, sericite and carbonates,
as one of the products of their saussuritization. ]\Iany cases occur in
highly granulated rocks, where it is almost impossible to say what is
primary, and what secondary epidote. Frequently, however, in rocks
which have sutfered extreme crushing, and are filled with secondary
epidote granules, large epidotes may be observed, broken and faulted
like the other constituents, proving that they existed before the rock
was subjected to the dynamic action.

Muscovite. Muscovite, — Both primary and secondary muscovite occur in these

gneisses, and it is often difficult in a particular instance to deteriiiine
to which of these two classes the mica is to be referred. Frequently
broad fresh laminie of muscovite are intimately intergrown with deep-
brown fresh biotite, and in such cases is undoubtedly of primary
origin.

The variety of the mineral referred to here is muscovite proper,
occurring in broad plates or laminje, as distinguished from the fine
scales of sericite resulting from the alteration of plagioclase, etc. It
possesses the usual bright polarization colours and other physical
characters common to the species, and no unusual features were
observed in the specimens examined.

CMilciritc Chlorite. — (Taken as a general group name). — This is the common

^'''^"''' alteration product of the biotite and hornblende of these rocks. It

polaiizes in the usual dull bluish tints.

Many of the gneisses owe their green colour to this mineral, which
gives them a very deceptive appearance, acid granitic rocks very often
closelj' resembling, at first sight, some massive altered basic irruptive.

I'vnte. Pyrite. — Is of common occurrence in all the gneisses, particularly

in the more basic ones. The red and brown oxides of iron which so
frequently stain the rocks can often be traced to this source.

Calcite. Calcite. — This mineral is abundant where alteration of soda-lime

felspars has proceeded to any extent. In such cases it forms large
irregular, brilliantly polarizing patches throughout the thin section.

Its abundance in some specimens, e. g., in the hornblende-granite-
gneiss from the south end of Opimika Narrows, is rather remarkable,
as this rock does not seem to have been greatly altered. In such
instances it may possibly be of primary origin.

Seiicitt. Sericite. — This is an abundant product of the saussuiitization of the

felspars, forming tine, brilliantly polarizing scales, intimately associated

with zoi
as serici
as it is c
microsco]

Apatitt
basic gne
and slend
less rounc
character]

Titaniti
served in i
size, deep
usual in su
colours to

The mir
position ho
grains of vj
tioned. Li
and also inc
grained grf
nearly all tl

Zircon.-^
The crystals
embedded ir
pleochroic h

Garnet. -

gneissic rock

certain locali

gneiss contai

basic-gneissic

and aggregate

pinkish coloi

elsewhere bet"

instances, all I

crystals were

Magnetite.-
granitic gneiss
few instances

H(rmatite.~
witli hexagona
along the clea\

•]

PETROGHAPHT OF THE LAURENTIAN.

85 I

with zoisite, epidote, calcite, etc. Some of the material referrtd to
as sericite in the description of these rocks may possibly be talc,
as it is difficult to distinguish between these two minerals under the
microscope.

Apatite. — This mineral is of frequent occurrence in the acidic and Apatite,
basic gneisses. It is mostly in the form of stout and short or long
and slender prisms, but grains with extremely irregular, and more or
less rounded outlines also occur. The large stout prisms are especially
characteristic of the diorite-gneisses.

Titanite (Sphene). — Remarkable crystals of this mineral were ob- Sphene.
served in some of the rocks examined. They are of unusually large
size, deep clove-brown in colour, and intensely pleochroic, and, as is
usual in such dark-coloured varieties, exhibit their brilliant interference
colours to perfection. Twinning was frequently observed.

The mineral is especially abundant in those rooks in whose com-
position hornblende occupies a prominent place. It occurs in irregular
grains of varying size, as well as in the well formed crystals just men-
tioned. Little crystals were observed penetrating the epidote crystals
and also included in hornblende and biotite. It frequently forms fine-
grained granular aggregates of '"onsiderable size, and is present in
nearly all the rocks described, both basic and acidic.

Zircon. — This mineral is also of widespread occurrence in the gneisses. Zircon.
The crystals are usually well developed, and often of large size. When
embedded in the biotite or hornblende it is usually surrounded by a
pleochroic halo.

Garnet. — This is by no means as abundant a constituent of the Garnet,
gneissic rocks of this region as was formerly supposed, although in
certain localities it is extremely plentiful. It occurs in the granitite-
gneiss containing cyanite, and also in several of the more or less altered
basic-gneissic hornblende rocks. It is usually in fresh irregular grains
and aggregates, frequently of large size, much fractured, and of a light
pinkish colour in thin sections. The optical anomalies which have
elsewhere been frequently noted, were not observed in the present
instances, all the grains appearing to be completely isotropic. Distinct
crystals were very rarely seen.

Magnetite. — As staced elsewhere, the scarcity of iron ore in the Magnetite
granitic gneisses is a remarkable feature in their composition. In a
few instances isolated grains were tested and found to be magnetic.

Hcvmatite. — This is frequently present in the form of thin plates Hseniatito.
with hexagonal outlines, and in irregular scales. It is often developed
along the cleavage planes of the biotite.

Stlfl"

i'i

■••'"-'•'^"•■"''"■(*'-'1'l'

86 I

NIPI8SINO AND TBMISCAMINO RBOION.

Ilinenite. Ilmenu Jreiierally s[ieaking, this is the iron ore which is present

in the diorite-gneisses, and is almost invariably accompanied by its alter-
ation product, leucoxene. It may be regarded as one of the essential
ingredients of these rocks. The peculiar brownish tints so often seen in
the plagioclase, are probably very often due to dust-like particles of
this mineral included in them.

Leucoxene. Leucoxene. — This is always an alteration product of titanic iron ores

or rutile. The grains of ilmenite are sometimes completely replaced
by whitish or yellowish, almost opaque masses of this mineral. A
peculiar cross-hatched structure was sometimes observed, probably due
to sagenitic growth of rutile which previously existed in the ilmenite
individual from which the leucoxene was derived.

Limonito. Liraonite. — The irregular deep-brown stains which frequently per.

meate the various minerals, especially the felspars, are probably in
most cases, due to the presence of this mineral.

Zoisite. Zoisite. — Accompanies epidote as the result of saussuritization of the

felspars, usually in quite small individuals which present no unusual
features.

Talc. Talc. — In a few of the more squeezed and altered gneisses, scales

were observed which seem to correspond in their general characters
with this species, as distinguished from sericite, but it is difficult to
discriminate between these two minerals.

Tourmaline. — Two or three columnar strongly pleochroic individuals
of this mineral were observed in one of the gneisses examined.

AUaniie. — Whilst not particularly abundant, many good examples
of this mineral were observed, more especially in those granite-gneisses
in which idiomorphic primary epidotes are plentiful. It occurs in the
reddish-brown pleochroic individuals in the centres of epidote crystals
with which it is in parallel orientation. These occurrences are of pre-
cisely similar character to those described by Hobbs in the Maryland
granites.

Rutile. Eutile. — This mineral was observed in a few instances in the form of

very minute, slender neeuLs penetrating the biotite.

Cyanite. Cyanite, — Occurs in rather short flat-bladed crystals, which rarely

show sharply defined faces in the prism zone, commonly forming
irregular columnar individuals. A few of the smaller crystals show
terminati jns, but with very rough faces.

The colour is usually of light-bluish or greenish, but occasional
crystals show a deep blue centre with a white margin. Some indi-

Tonrmaline.

Allanite.

BARLOW

vidua
devel(
and c(
rock i
are ol
biotite

Unc
colourl
These ]
not not
parallel
longitU(
As is ii]

Orap,
gneiss, i
lines. ,
in diamt

Fihrol
lected i
vicinity i
and thesi
which aci
pitie statj

Augite.

absent frc

In certair

tion prodi

but this

examined

no certain

observed 1

darker col(

The nai]
1863* by
extensively
Ottawa in t
These were

Geology

ORENVILLE SERIES.

87 I

viduala measure half an inch across and an inch in length. It is best
developed in those portions of the rock which are free from biotite,
and consequently of a lighter colour. In the darker portions of the
rock it is frequently intergrown with the biotite. The individuals
are often bent and hold many inclusions, particularly of pyrite,
biotite, quartz and graphite.

Under the u)icroscope the sections are transparent, and generally
colourless, but patches of a light-blue colour occur here and there.
These patches exhibit a pleochroism (light-blue to colourless) which is
not noticeable in the colourless portions of the crystals. The cleavage
parallel to M and T do not traverse the entire section as a rule. In
loni^itudinal sections the parting parallel to P is also clearly shown.
As is invariably the case, the cyanite is accompanied by garnet.

Graphite. — This mineral occurs in some quantity in the cyanite- Omphite.
gneiss, in the form of irregular Hakes, rarely with rude hexagonal out-
lines. A few flakes were observed to be nearly a quarter of an inch
in diameter.

Fibrolite. — Only a few specimens of the cyanite-gneiss were col. FibroHte.
lected from the cuttings on the Canadian Pacific Railway in the
vicinity of Les Erables Rapids and Snake Creek, on the Ottawa River>
and these show no fibro^:'^,', but it is almost certain that this mineral,
which accompanies the cyanite in the similar rock from near Wahna-
pitse station, will be found associated with it in the area.

Augite. — This miner.al, as elsewhere noted, is almost, if not entii'ely, Angite.
absent from those gneisses which have been microscopically examined.
In certain specimens a few skeleton forms, entirely filled with altera-
tion products, were observed, which may originally have been pyroxene,
but this is by no means proved. The hornblende was carefully
examined to see if there were any traces of pyroxene cores in it, but
no certain evidence of this was obtained, although in some cases it was
observed that the exterior of tho hornblende individual was of a
darker colour than the central portion.

GRENVILLE SERIES.

The name Grenville Series was the distinctive title applied in origin of
1863* by Sir William Logan to the series of crystalline rocks so "*'"®*
extensively and well exposed in the region on the north side of the
Ottawa in the vicinity of the Augmentation and village of Grenville.
These were referred to as Middle Laurentian and supposed to con-

•Geology of Canada, (18C3), p. 83!t.

ISP
KM I

S- 1

SSS

!■■

88 I

NIPISSINQ AND TEMI8CAMINO REGION.

ceptions.

formably overlie the Lower Laurentian or Fundamental (Jneiss. The
rocks thus classified comprise a great variety of gneisses with
which are associated considerable volumes of crystalline limestone,
and a detailed map was published showing the distribution of the
component bands.* Many reasons were adduced as evidence for
regarding the whole series as greatly metamorphosed sedimentary
Early miscoti- strata. These proofs had reference chiefly to the banded or foliated
character of many of the composing masses, believed to represent
the surviving traces of the parallelism due to original sedimentation,
the pi'esence of large and important beds of limestone, together with
the occurrence in some of these bands of forms described as represent-
ing organisms of low type. Subsequent examination in the field, sup-
plemented by the detailed petrographical studies rendered possible
by the recent perfection of the microscopic methods of research, have,
however, revealed the fact that, while certain of the fine-grained, light-
grayish, rusty-weathering gneisses are closely allied instructure and com-
position to ordinary shale or slate, other rocks, representing a very
much greater volume of the whole series, are undoubtedly the foliated
equivalents of the ordinary plutonic irruptives.f

In the area covered by the accompanying map-sheets, the line of
subdivision between what has usutally been regarded as Lower Lauren-
tian and the Grenville Series, was described by Sir William Logan, in
1844, as occurring somewhere in the vicinity of the Mattawa River.
The supposed line of boundary was based on the occurrence at certain
points of isolated masses of crystalline limestone, but these have since
been found to be in intimate association with rocks which are believed,
with some confidence, to be the foliated equivalents of ordinary
granites and diorites.

In the area under description, only one very limited occurrence of
the fine-grained and evenly banded light-grayish gneisses usually associ-
ated with the Grenville series was noticed, consisting of a small band
interfoliated with the ordinary reddish granite-gneisses, a little over
two miles east of Rutlierglen station on the Canadian Pacific Railway.
The strike of this band is about N. 20° W., with a dip to the north-
east at a high angle. The hand specimen represents a fine-grained
evenly foliated, rusty-weathering, grayish, graphitic gneiss. Under the
microscope, it is a fine-gr-^'ned admixture of interlocking grains of fels-
par, quartz, and a rather pale-coloured bleached biotite, together with
smaller quantities of pyrite, graphite, rutile, and a mineral closely

* Atlas, Geology of Canada, (18(53), Map No. 1.

fAdams. A Further Contribution to our knowledge of the Laurentian, Am.
Journ. Sci., July, 1895.

Logan's
line of su
divisiou.

Rocks of
Grenville
.Series.

■. ■ I

•]

OKENVILLE SERIES.

89 I

resembling zoi.site in minute prismatic crystals, arranged in nests com-
posed of aggregates of crystals and crystal fragments running parallel
with the foliation. The rock has evidently been subjected to intense
and long continued dynamic action, the foliation being pronounired,
while the recrystallization has been so complete as to mask much of its
original structure. It bears a marked microscopical as well as macro-
scopical resemblance to the sillimanite gneisses described by Dr.
Adams.*

The most important band of crystalline limestone noticed in the whole Crystallinfi
district, occurs at the foot of Lake Talon, an important expansion of j^^j^^ TiJon.
the Mattawa River. The presence of this band was first noted l)y
Bigsbyt in 1820, and later in 1844, by Logan. Dr. Bell, in 187G, also
gave a short description of its mode of occurrence. \ The rock consists
of whitish crystalline limestone with small thickly disseminated specks
and patches of green serpentine. It is first noticed on the south side
of the lake a short distance above the outlet, occupying the points along
the shore, while the massive reddish granitite-gneiss rises into rounded
hills behind. The limestone, as far as can be ascertained on account of
the massive texture of the gneiss, occurs as an interfoliation, (lipping
S. 8° E. < 25. Farther down, towards the chute, the rock contains a
good deal of serpentine in addition to some other impurities, and occurs
seemingly as a large irregular rounded patch in the gneiss. At the
narrows, a short distance above the Talon Chute, the contact between
the crystalline limestone and massive rather indistinctly foliated red
granite-gneiss is well shown, the former dipping N. 74° E. <20° while
the latter, with a nearly east-and-west strike overtops or flows over
the mass of the crystalline limestone, the indistinct foliation of the
gneiss conforming in general with the line of junction between the
two rocks. See Fig, 1.

Fig. 1.

Skktch mkction siiowixt; stuuctuhk of crystai.li.vk limestone (a) .-^Nn massive

RED (iUANrriTK (INEISS (b) NEAU TaLON ChL'TK, ^IaTTAWA RiVEU.

*Aimual Report, (ieol. Surv. Can., vol. VIII. (N.S.) Part j.

tShoe and Canoe, vol. I. London, 1850.

JReiKirt of Progress, Geol. Surv. Can., 1870-77, p. 207.

,.^..

IMAGE EVALUATION
TEST TARGET (MT-S)

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Photogr^hic
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23 «VI«'' MA»N STRUT

WEBSTER, N.Y. i4S«0

(716) 873-4503

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Aljroiikmii

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90,1

NlPISSIJta AND TEMI8CAMINO REGION.

At the Talon Chute, there are two channels by which the lake
discharges into the gorge below. The largest of these channels is
situated near the north side, while the southern one has been excavated
along a band of ophicalcite, seventy feet in thickness intercalated
with the gneiss and dipping in a southerly direction <25°.

Smaller bands and patches of crystalline limestone, likewise occur on
three of the Manitou group of islands in the eastern portion of Lake
Nipissing. On the west side of the most southerly of these islands, beds
of a beautiful light salmon-pink crystalline limestone occur, containing
radiating crystallizations of dark-green hornblende, black biotite, and
yellowish-green epidote. The strike is about N. 80° E. and the angle of
dip is about 65°. This is associated with the prevailing rather fine-
grained dark-reddish and green granitite-gneiss.

On the east side of the Great Manitou Island (Newman Island) a
few chains south of the north-east point, there is a layer or bed of
pinkish limestone, weathering yellow, reddish and grayish. The strike
of the dark-red and green granitite-gneiss is about S. 60° E. and the
dip south-east < 45°. On the west side of the most easterly of the
Manitou Islands, about the centre of the island, beds and patches of
pinkish and whitish limestone are embedded in the dark-red and green
granitite which has a strike of S. 5° E. and a dip to the east <45°.

HURONIAX.

The name Huronian, was adopted by Sir William Logan and Dr.
T. Sterry Hunt in i855,* to include the clastic rocks believed to
overlie the Laurentian gneisses in the districts adjacent to Lakes
Huron and Superior.

The area included by the present report, exhibits large tracts of
country underlain by pyroclastic and epiclastic rocks identical in
lithological character with those described as Huronian by Murray in
1850. It forms, in fact, the north-easterly extension of the same belt,
which has been traced with practical continuity from what is gen-
erally termed the " typical " area on the north shore of Lake
Huron. The inclusion of these rocks under the name " Algonkian,''
shows a tendency on the part of some geologists to revert to the
erroneous grouping of Huronian, Animikeand Keweenawan as integral
portions of a single system or series of formations, in spite of the pro-
nounced hiatus known even then to exist, though perhaps not appre-
ciated to its full extent, by Sir William Logan. As has been pointed
out by Dr. Dawson t and others, the proposed use of the term

•KHquisse (.T(''ologique dn Canada. Paris, 1855, p. 29.

+Prt'»idential Address to the Geological Section B. A.A.S., Toronto meeting, 1897

BARLOW.

Algonl

leading

not on,

over ex

rocks, a

which ti

needless

rocks he

have be

since the

the vari<

It is als(

further

nations c

ching ser

TheH
the norti
admit of
one anotl
perfect ti
occur for
clinal folc
where cor
result of tl
glomerate,
usually sul
etc., embec
state of di
scales and
considerab
tion produ
This rock }
erate "or "
used by Lo,
dark greeni
any fragmc
above into i
similar con
character, t
instances wi
the colour s

•Report of I

■]

HURONIAX.

91 I

Algonkian in the same extended sense is both unnecessary and mis-
leading, and it should therefore be deprecated. Its adoption disregards
not only the zealous and accurate work of many trained observers
over extended areas characterized by the presence of these Archiean
rocks, and would also supplant a useful and well known term, of
which the priority remains unquestioned, by a name which is at once
needless and indetiiiite. No attempt has been made to correlate the
rocks here described as Huronian with certain series or groups which
have been lately and ably reported upon under the new conditions
since the use of the microscope has made an accurate description of
the various component rock masses not only possible but imperative.
It is also regarded as premature as yet to anticipate the results of
further and more complete microscopical and stratigraphical exami-
nations of the Huronian, Grenville, Hastings, Keewatin and Coutchi-
ching series.

The Huronian rocks, which are extensively and widely developed in
the north-western part of the region under description, naturally
admit of a three-fold subdivision, the component members following
one another in undisturbed succession, each showing a gradual and
perfect transition upward into the succeeding member. The rocks
occur for the most part in slightly undulating anticlinal and syn-
clinal folds, except in the vicinity of certain large irruptive masses,
where considerable disturbance as well as alteration is found, as a
re-iult of their intrusion. At the base of the series is a breccia-con-
glomerate, containing pebbles and fragments, often angular, though
usually subangular or rounded in outline, of granitite, diabase, diorite,
etc., embedded in a matrix composed of the same materials in a finer
state of division, while the more minute interstices are filled up with
scales and flakes of chlorite and sericite. Where this matrix forms a
considerable portion of the rock, the abundance of these decomposi-
tion products gives a prevailing dark-green colour to the whole mass.
This rock has in previous reports been referred to as " slate conglom-
erate " or " chloritic slate conglomerate," a name first proposed and
used by Logan.* This coarse fragmental rock passes upward into a
dark greenish-gray greywacke or felspathic sandstone, in which few if
any fragments are macroscopically apparent. This in turn merges
above into an exceedingly compact and fine-grained rock of essentially
similar composition, which gradually assumes a banded and slaty
character, the planes of cleavage, when present, corresponding in most
instances with the evidences of original sedimentation as revealed by
the colour stripings. Superimposed upon these, usually without any

•Report of Progress, Geol. Surv. Can., 1845-4(5, p. 67.

No attempt
made at
correlatiiiu
with otlitT
Archil-ail
groujii?.

Position and
composition
of l)r('ccia-
uongloiuurate.

(4reywacke.

Slate or shale.

i'li:

! I;

iii ';i

92 I

NIPISSINO AND TEMISCAMING REGION.

Earl^
opinions
alHiut tlie
source of
Huronian
sediments,

Quartzite- sharp line of division, although at times there is an abrupt change, is
grit or arkoHe. j^ quartzite-grit, made up chiefly of fragments of granitic quartz with
some of felspar, all usually more or less rounded and containetl in a
felspathic matrix, now largely altered to yellowish-green sericite.

The rock is generally yellowish-green in colour, owing to the abund-
ance of sericite, the scales of which are often macroscopically apparent
in the matrix. On this account it has been usual to refer to the rock as
a sea-green quartzite. Occasionally it is of a flesh-red colour, when it
is with difficulty distinguished from ordinary granite. It occurs in
massive much jointed beds, the stratification at times being shown only
by a parallel disposition of certain coarser or conglomeratic bands. It
is occasionally fine-grained but usually approaches the character of a
grit or fine conglomerate.

Until very recently, it was a matter of general belief, based on pre-
vious descriptions and reports, that the .source of such clastic material
was to be traced to the breaking down of the gneissic or foliated
crystalline rocks usually classified as Lower Laurentian. The writers
repeatedly insisted that gneissic pebbles, distinctly referable to the
Laurentian, formed the most abundant coarse fragmentary material in
the basal beds of the Huronian. Later geological research in this and
neighbouring Archiean areas has shown, however, that such state-
ments are largely erroneous, as foliated fragments are only very
occasionally represented and in most cases are entirely absent,
while those of a somewhat coarse-grained aplitic granite make up
the greater portion of many of these conglomeratic rock masses.
The examination likewise of the line of junction between the
gneisses and the granites constituting the Laurentian of this district on
the one hand, and the breccia-conglomerates and slates of the Huron-
ian on the other, has shown that the former were in a plastic or softened
condition after the hardening of the Huronian sediments.*

Most geologists were inclined, despite these opposing facts, to believe
that the Laurentian gneisses and granites constituted the original floor
or ba.seuient upon which the Huronian sediments were deposited and
from which their material was derived. The present attitude of these
rocks, moreover, was explained as due to the instalnlity of the earth's
first -formed crust allowing and favouring a settlement of any overlying
clastic material, accompanied as it must have been by frequent and
repeated upwellings of the molten magma from beneath. These
unsettled conditions were further accentuated by extensive fracturing

and en
binintr
aloiiij
rocks.

Care

baseine

but app

they ha

complex

islands j

Tliessalc

the intei

which tb

pierces a

show f,'Iei

the pebb

In spit
junction
anticipate
Lauren tia
be ultimal
to the nor
the authoi
clastic cha
Huronian.
represents
ejectament
ocean, and
of aqueou
intimately
aqueous ere
difficult if
tained in
posed of
tinctly refei
surface in
of this coai

* Vide ante, also American Geologist, July, 1890,
Am., vol. IV., pp. 313-:«2.

PI), in-32. Bull. Geol. Soo.

Am. Jouri
XXXIV, 1887

tAm. Journ
vol. IV., pp. a

BARtOW.

HUKONIAN.

95 I

and crumpling as a result of the earth's secular refrigeration, all com.
bining to bring about the conditions and phenomena now witnessed
along the lines of junction between the Laurentian and Huronian
rocks.

Careful search has been made for localities in which the underlying
basement might have escaped this seemingly wide-spread disturbance, aii'l'van'^Iisi'

but apparently in vain. Pumpellvand Van Hise"' have (lescril>ed what •If'^tiiptiou of
,,,,,,,, . ,, , , contact near

they have called a basal conglomerate reposing upon a ruivdamental Thessalon.

complex of crystalline schists and granite, as exhibited on two small

islands near the north shore of Lake Huron, a short distance east of

Thessalon, Ontario. A difference of opinion, however, exists concerning

the interpretation of this section, and the fact th.it the granite from

which the pebbles in the conglomerate are believed to have been deri\ ed

pierces and alters the slaty rock overlying the conglomerate, seems to

show <;learly that the correlation of this granite witli that constituting

the pebbles in the conglomerate is decidedly at fault, t

In spite, however, of the generally irruptive character of the line of Intmsivo con-
junction between the Laurentian and Huronian, it was confidently Hj^,r,,ni'ui' i'ml

anticipated by even those who believed in the intrusive character of the liininntian
T . ... , 1- 1 , 11 iiotiiccesftaiily

Laurentian gneisses that, in some place an undisturbed contact would universal.

be ultimately found. The detailed geological examination of the region
to the north-east of F^ake Huron, carried on for the last ten years by
the author of this report, has furnished abundant prof)fs of the pyro-
clastic character of the rocks composing the two lower members of the
Huronian. The breccia-conglomerate, greywacke and slates evidently
represented the graded forms resulting from the consolidation of volcanic
ejectainenta showered out and spread upon the bottom of a shallow
ocean, and there somewhat rounded and otherwise modified as a result
of acjueous action. In many ca.ses, however, these rocks are so Huronian
intimately associated with materials resulting from proces.ses of ordinary "'■"'^' "l>
aqueous erosion and deposition, that, in most instances it is extremely pyroclastic
difficult if not impossible to make a separation. The fragments con- '^1"'.^!!,.''"^ "*" '^
tained in the breccia-conglomerate are, as has been shown, com-
posed of rocks of igneous or plutonic origin and in no way dis-
tinctly referable to any Laurentian strata now exposed at the earth's
surface in the same area, while the fre([uent intimate association
of this coarse fragmental rock with large masses of diabase, gabbro and

*Am. Journ. Sci., III. vol. XLIII, pp. 224-232, March, 1892; also III. vol.
XXXIV, 1887, pp. 207-216.

tAin. Journ. Sci., III. vol. XLIV., 181t2, pp. 230-23y; also Bull. (ieol. Soc. Am.
vol. IV., pp. 330-332.

i Kili

i'in'itj smu nntrt(

h \

if ■ ^

1 •
■

A true
haseniunt or
fundamental
granite on
Lake Temin-
earning^.

94 I

NIPIS8INO AND TEMISCAMINO REGION.

granitite, cannot be regarded as merely accidental. The earlier part
of the Huronian period in this district was evidently a time of intense
and long continued volcanic activity, and the greater portion of the
rocks representing this lapse of time are pyroclastic in character.

True sedimentation on a large scale seems only to have been ushered
in toward the close of the period, and the quartzite-grits and con-
glomerates prevailing towards the summit of the series are very typical
examples of epiclastic material.

The relations found to exist between this arkose and an underlying
fundamental biotite-granite or granitite, as exposed on either side of
Lake Temiscaming in the vicinity of Bale des Peres, indicate its deri-
vation to be a result of the disintegration and degradation in situ of
the underlying granite, showing a gradual and uninterrupted passage
outward and upward from the parent mass. The nature and import
of this passage were the subject of an illustrated paper, prepared by
the author and Mr. W. F. Ferrier and presented at the Toronto meeting
of the British Association for the Advancement of Science in August
1897.* A short resume of the interesting phenomena observed has
already appeared in the Geological Magazine,f but the details, not only
of the field relations of these rock masses, but also of the petrographical
examinations will be found in that portion of this report dealing with
the geological description of Lake Temiscaming. The relations be-
tween this granite and arkose are of rather unusual scientific interest,
showing as they do the pre- Huronian existence of a basement or floor
upon which these sediments were laid down and which in this portion
at least has escaped the movements to which the Laurentian gneisses
have been subjected.

The petrographical studies undertaken with the object of determining
the origin, composition and minute structures of the various rock
masses making up the bulk of the Huronian, have been so numerous
and detailed that it is impossible in the present report to give at length
the description of each separate slide, especially as many of these pre-
pared from specimens obtained at widely separated localities, were after-
wards ascertained to represent rock^ presenting no essential points of
difference. It will therefore doubtless be found sufficient to give a
general description of each of the three members constituting the
Huronian, at the same time pointing out the nature of the transitional
sequence so frequently witnessed from one rock to the other.

* On the Rt'lationH and Structures of certain Granites and Associated Arkoses on
Like Temiscaming, Canada, Kep. B. A. A. S., Toronto, 1897, pp. ()6()-G(iO.

+ Geol. Mag., New Series, Decade IV., vol. V., No. 1, pp. 39-41, January 1890.

MNLOW.

The roc

or "chlori

described

Lake Tern

indicates n

nature am

is applied

is usually (

ing in prop

ducts whic

weathers fr

surfaces no

a light oli

layer, usual

pale-yellow

usual sausst

quantity of

massive, sh

tion, while t

rogeneous m,

degree of cer

however, it h

this is in m(

planes, which

usually at vei

the line of ou

lar curving li

pressure, simi

resulting frott

in many descr

been repeated!

the frequent a

Although til
rock occasiona
is no necessar
rock varies wid
exceedingly ha
chlorite and oth
are so soft that
and in its more

MRLOW.

HUROMAN.

95 I

Breccia-conglomerate.

The rock tlius designated is identical with the " slate conglomerate "
or "chloritic slate conglomerate" of the earlier reports of the Survey,
described h\' Logan as following the Laurentian orthoclase-gneiss on
Lake Temiscaming. The new name, as proposed, is preferred as it
indicates at once what is now confidently believed to bo the true
nature and origin of the large and important rock masses to which it
is applied. This rock, especially where the finer matrix is abundant,
is usually of a dark-greenish or greenish-gray colour, the colour deepen-
ing in proportion to the (juantity of the greenish decomposition pro-
ducts which may have been developed. The immediate outer coatitig
weathers from yellow through brown to almost black, although certain
surfaces not exposed to the continued action of the atmosphere retain
a light olive-green appearance. Beneath this dark outer surface, is a
layer, usually about one-eighth of an inch in thickness, composed of
pale-yellowish decomposed material which evidently represents the
usual saussuritic products resulting from the alteration of the large
(juantity of felspar present in the rock. As a rule, the rock is extremely
massive, showing little or no evidence of lamination or stratifica-
tion, while the coarser fragmental material is arranged in such a hete-
rogeneous manner that it is exceedingly difficult to ascertain with any
degree of certaintj' either the angle or direction of dip. Sometimes,
however, it has a slaty or foliated structure as a result of pressure, and
this is in most cases the only structural feoture discernible. These
planes, which evidence intense and long continued pressure, are inclined
usually at very high angles, the strike corresponding in direction with
the line of outcrop of neighbouring intrusive masses, while the irregu-
lar curving lines of foliation produced by the unequal resistance to
pressure, simulate in a most marked manner the uneven lamination
resulting from original bedding. It is, therefore, not surprising that
in many descriptions of exposures of similar rocks, such a structure has
been repeatedly mistaken for stratification, the descriptions asserting
the frequent and usual highly tilted character of these rocks.

Although the slaty cleavage, especially in the upper portion of this
rock occasionally corresponds with the original stratification, there
is no necessary connection between the two. The hardness of this
rock varies widely, the least altered or more quartzose varieties being
exceedingly hard, while those exposures in which a large amount of
chlorite and other greenish decomposition products have been developed
are so soft that they can be readily scratched. Both as a massive rock
and in its more imperfect forms of slaty structure, it exhibits the char-

Breccia-con-
glniin-rate or
nlatf coii-
ffloinenitf
of Lugaii.

Colour and
structure of
broccia-pon-
glnincratt?.

Fra(n»PHta
niaking up
bri'ccia-con-
gloinerate.

rr-

96 I

NIHlSSINd AND TKMI8CAMING REGION.

Not littoral
in ori);in.

I'yi'iL'liistic

IllltlllC ..f

1 1 r
1 1

l)rfcci:l-ei)li-
glciiieiiite.

i'i

Comin)fiti()U
of matrix of

hri'cciii-coii-
gliiiiicrate.

acter of a conglomerate, carrying fragments of various irruptive mate-
rial which vary in size from the smallest pebble to some boulders a
foot or even more in diameter. In some localities, the rock is so full of
these fragments that very little of the finer interstitial matrix is appa-
rent, while in other places only an occasional one is found. Usually
the fragments are more or less perfectly rounded ; often they are sub-
angular, while in some outcrops these larger individuals present sharp
and often i-e-entering angles. The breccia-c<jnglomerate presents all
the characteristics usually assigned to a rock resulting from the
consolidation of an ordinary littoral deposit derived from the break-
ing down of an area of irruptive rocks of both acidic and basic com-
position. The wide area, however, over which the rock is distributed,
the composition and outline of many of the larger individuals, as well
as the frecjuent intimate association with large masses of diabasic and
gabbnnc rocks, are incompatible with such an interpretation of the
manner of its formation.

It is often exceedingly difficult to distinguish between true conglo-
merates or thi ) representing the solidification of extremely local shore
deposits, and agglomerate-breccias which may have a much more
widespread distribution, but in some instances the most typical con-
glomerate phase, containing perfectly rounded and seemingly water-
worn fragments, has been traced directly and continuously into areas
in immediate conjunction with the parent masses, where the contained
fragments show no sign whatever of aqueous abrasion, the rock being
a typical breccia. Many of the fragments moreover are composed of
material v/hich has probably been derived from beneath as a direct
result of violent explosive action, as they cannot possibly be connected
with any rock present at the surface in the region adjacent to these
exposures.

The finer-grained portion, or matrix, of the least altered phase of this
rock, possesses a rather typical clastic structure, although many of
the fragments are often so irregular and angular in outline as to indi-
cate clearly that they have not suffered the rounding or trituration to
the extent that ordinary elastics of this kind exhibit. The rock is
seen to consist mainly of granitic debris, the majority of the fragments
being simple minerals ; although coarser phases show occasional com-
posite rock individuals. The minerals usually noticed are orthoclase,
plagioclase, and, more rarely microcline, embedded in a still finer-grained
ground-mass of these same constituents, together with chlorite, sericite,
epidoteand zoisite,and occasional granules and broken crystals of zircon,
sphene and apatite. Biotite and more rarely hornblende, both largely
altered to chlorite, may also be sometimes distinguished, but fresh indi-

BARLOW 1

viduals b

very frofj

through t

brilliiintji

in various

ite. Unit

usually in(

characteri

black opaf|

In several

i'ly the in

Occasional

of decompc

The (juai

ordinary g(

nouncod de

.Some of th(

tiie individ

marked turl

products of (

Most if not i

the alteratio

many of the

posed to this

Fragments o

abundant.

almost inva

biotite, altho

Jilly present.

scales or mat

■'ire sumetiin(

colouiloss to

nation betwe(

•'IS a finer int«

and felspar gr

and crystals, i

which is usua

lowisji colour

fi rule, compos

ing their ori<q

ved, are rarely

coarseness of s
7 ^

■ARIOW

HURONIAX.

97 I

viduals belonginj^ to these species are rather unconiinoii. Pyriteisa
very frefjuent and often extremely a^juiidant constituent, diHtributed
through the rock in irregular grains and masses, hut soinctinies also in
brilliant and well striated cuhos. In many instances it may be noticed
in various stages of its decomposition tf) hydrated oxide of iron or linion-
ite. Ilmenitc is likewise very often present, botii in grains and crystals,
usually more or less altered to leucoxene, and occasionally exhi))iting the
characteristic "gridiron " form of this decomposition. Magnetite, in
black opaf|ue particles and crystals is also rather commonly represented.
In several instances, broken fragments of crystals of tounnaliiie, show-
ing the intense dichroism peculiar to this mineral, were detected.
Occasionally also carbonate of lime is present as a secondary product
of decomposition.

The quartz is usually in clear more or less rounded areas and is tin (imrtz.
ordinary granitic variety. It fret;iiently shows, in a somewhat pro
nounced degree, the uneven or undulous extinction due to pressun-.
Some of the felspar fragments are rather fresh and glassy, but most of
the individuals show incij)ient alteration, consisting of a somewhat
marked turbidity arising from the development in thera of the \ arious
products of decomposition to which the name saussurite has been applied.
Most if not all of the sericite present in the rock has been derived from Sericite and
the alteration of the felspar, especially of the more minute fragments, '^'"'"■'t^'-
many of these present in the finest ground-mass being wholly decom-
posed to this form of hydrous mica, together with epidote and zoisite.
Fragments of felspar showing microperthitic intergrowth are rather
abundant. By far the greater proportion of the chlorite, which is
almost invariably present, has resulted from the decomoosition of
biotite, although some may have Ijeen derived from hornblende origin-
ally present. The sericite occurs for the most part in the minute
scales or matted aggregates, although occasionallj' in large plates which
are sometimes macroscopically apparant. The mineral varies from
colouiless to pale yellowish-green, showing brilliant chromatic poh.ri-
zation between crossed nicols. The chlorite and sericite usually serve
as a finer interstitial cement lilling in the spaces between the quartz
and felspar grains The epidote and zoisite occur in irregular granules
and crystals, the former polarizing in brilliant colours, while the latter,
which is usually in more perfect crystals, shows the deep bluish or yel-
lowish colour characteristic of this mineral between crossed nicols. As
a rule, composite fragments, made up of two or more minerals, occupy- r',,ini)<wit4!
ing their original positions in the rock from whose waste they were der'- f'''*^?''"'"*-''-
ved, are rarely seen in this tiner matrix, but with a progressive increase u
coarseness of grain, such fragments gradually appear. As a rule, ev( n
7

I r 1 '

,1 r. 1

i .'I

i .1

'■i^

JjMyi'T fnig--

IIU'lllH .111(1

btjiililfis.

Ci)niiinsiri(
<if gi'iuiititc

J)(lll)lfS of

bifccia.

08 I

NIPI.SSINfi AND TKMI8CAMINO REGION.

Description

diabasH

fratouenta.

when small, those rock-fragnionts possess a more rounded f»utlino tlian
individuals made ii|) of simple minerals which are very frequently
(juite sharp and an;.ai]ar.

Tn this matrixor <5i(*un(I-mass just<h'sciibe(l,are eu\bedded fraj,'ments,
pebbles and sometimes even boulders of bicMie-granite or ;;'ranitite,
hornblende-fjranite, diabase, dioritv> (?) quartzite and fire ;;rained slaty
j,'rey\\<tcl<t' or hiilleflinta-like rock, representing an extremely fine-
grained mosaic of felspar and quartz. Many of these larger fragments,
as is usual in similar s(jueez(Hl rocks, arc surrounded by a rim of sericite
and epidote, while occasionally, where tlie mass has been subjected to
intense pressure and pronounced pneumatolylic action, as on Ko-ko-ko
l^ay in Temagami Lake, the whole matrixh.is been altered to a hydromica
schist infiltrated witli secondary .silica, wliile the pelibles have undergone
considerable stretching and deformation. Gi-anitite pebbles and frag.
mcnts are by far the most abundant and are almost invariably present
■where outcrops of this rock occur. In occasional localities, indiviiluals
of diabase, which are next in point of general abundance, piedominate
over those of granitite. The granitite is usually of a distinct ilesh.
red or pink, sometimes reddish-gray and occasionally grayish colour.

It is commonly rather coarse in texture and more rarely pegmatitic.
Macroscopically it shows a preponderance of pinkish felspar, a much less
proportion of grayish translucent quartz and a sparing quantity of a
, greenisli ferro-magnesian mineral. A section prepared from one of the
pebbles obtained from an exposure on Gull Rock Islands in Lake
Temiscaming, showed the rock composing it to be greatly decomposed,
the felspar turbid, tilled with sericite, epidote and calcite and tlie bisili-
cates almost entirely altered to chlorite. Orthoclase apparently pre-
dominates, but plagioclase is abundant and microcline in small quantit}'
also occurs. The quartz is the ordinary granitic variety, full of inclusions,
and while pos><cssing a sf)mewhat wavy extinction does not show much
further evidence of having been subjected to very intense dynamic
action. A few little areas of granophyre were noted. The ferro-
magnesian constituents originally present, were probably both biotite
and hornblende, but these minerals have been so completely altered
to chloiite as to mask their ti-ue optical characters. The former mineral
doubtless predominated. The change to chlorite has been accompanied
by the deposition of much secondary magnetite. Ilmenite is also
present and is accompanied by leucoxene, while apatite is abundant.

J The diabiise fragments so frequently present are usufiUy very fine-
grained, although sometimes so coarsely crystalline that the ophitic
structure is distinctly discernible to the unaided eye. Occasional pieces

BARLOW. I

Still mor

sentalt(

decoiiqu

as comp

every ca

thin sect

in Lake

alteratioi

decompo?

til is adv

remains.

causing t

ai-eas betA

green vhh

alteration

scattered

much coai

revealing

decompose

matted a;

allot riomo

Tlie ilm
grayish nu
produced
pyrrhotite
nients and

In addit;

others npr

were noticf

ments of a

deveIo])ed i

also observe

fragments, i

which when

ance. Souk

chlorite groi

senting the

Temiscamini

pligioclase, a

turbid owin<>

composite fr

•J

IIUKONIAN.

99 I

still more coarsely ciystallint* luul holncrystnllint' in struetuift niuy repnv
sent iiltercd galihros or diorites, but tins ferro-inagnosiaa niiiH'rals are all
decomposed to chlorite. These ])el)bles luo identical witli those descriljod
as composed of a "greenish t'elspathic rock '" in earlier rt'iKirts. In
every case examined they were foiuui to lie niii -h decomposed. A
thin section of a fine-grained peblile, also from the (iull Rock Island
in Lake Temiscaming, shows the rock to have undergone great
alteration, the felspar being saussuriti/ed and the original augite
decomposed to a pale-greenish chlorite. In spite, however, of
this advanced alteration, t!ie typical ophitic structure (jf diab.ise
remains. Occasionally some of the felspar has a broad iabular habit
causing the rock to approach the gabbros in structure. The irregular
an.'as between the plagioelase laths are filled with a felled mass of pale
green chlorite scales. Leucnxene, re>,uUing from the almost complete
alteration of the ilmenite originally present in the roek, is plentifully
scattered through the section. Other sections examined, ijelonging to
much coarser grained fragments, were of essentially similar composition,
revealing the .same advanced alteration. The laths of j)Iagif)clase,
deoompo.sed to a partially opaijue gray saussuritic mass, penetrated a
matted aggregate of pale-green clil')rit.e scales representing the
allotriomorphic areas of augite originally present.

The ilmentite has wholly disappeared, to be replaced by opaque
graj'ish masses of leucoxene, showing the characteristic skeleton forms
produced by the rhombohedral parting. Pyrite and occasionally
pyrrhotite and chalcopyrite are constituents of these diabasic frag-
ments and pebbles.

In addition to these peV)bles and fragments of granitite and diabase,
others representing a greatly crushed and stretched felspathic (juartzite
were noticed, containing also sericite and chlorite. Occasional frag-
ments of a rock in which plagioelase and orthocla.se are porphyritically
develojjed in a tine-grained granular quartz-felspar groundraass were
also observed. Besides the.se composite pebbles, there are very often
fragments, usually sharply angular in outline, of both felspar and quartz,
which when present alone give the rock a decidedly porphyrite appear-
ance. Some of these pseudo-phenocrysts embedded in a dark-green
chlorite groundmass were examined, the rock thus constituted repre-
senting the " country-i'ock " of Wright's mine on the east side of Lake
Temiscaming. Some of these individuals proved to be felspar, chiefly
plagioelase, which have a broad tabular habit, well striated and very
turbid owing to somewhat advanced decomposition, while others are
composite fragments of some porphyritic granitic rock with the large

Otiipr
flagliii'llts
pli'sellt iu

bri "ccia.

mmmm

100 I

NIPISSINfi AND TEMISCAMINO HKQIOV.

ili-triliiitiim nf
l)rcccia

TrnriKitiim
u|>\vnrtl to
^'^ey\Vilckt■•

crystals of wol! strinted plas^ioclase surrounded l)y finely fir.inulatcd
(|uartz.

Tliickins.Hiinil As will bo spcn by a roft'reni'o to tlin acconiiiaii\ in;,' map slieets, this
brecx-ia-conf^lonionito is of very widespread occurienco in this district.
On Lake Teniiscaminf,' it rises into hills nearly five hundred feet in
height, in thick, almost structureless masses, altliou^'h in large and well
exposed sections, lines which evidently represent original bedtling may
be distinguished. The total volume seen cannot be much less than six
bundled feet, which perhaps represents the givate.«t thickness attained
by this rock, although the conditions under which it must have been
deposited were necessarily so unstable that at no place can the basement,
upon which it originally rested, be detected. The present nature of
its contact with rocks which may possibly represent re-fused portions of
this original basement, shows evidence f)f a considerable sinking down
of the mass of clastic material into the molten or plastic magma beneath,
so that it is manifestly impossible to state the true total thickness of
what has Ijoen regarded as the basal member of the Huronian.

This breccia-conglomerate passes upward into a dark-greenish com-
pact rock closely related in composition with the finer grained portum
or matrix of the much coarser fragmental rock beneath. The transition
upwards consists mostly in a gradual loss of the larger composite
fragments.

ComiKmitiiiii Although in certain places an occasional pebble of reddish biotite.

of gnywacki.' granite may bo noticed, sections of t'lis fine-grained and compact grey-
wacke or felspathic sandstone show an even-grained mixture of angular
and subangular fragments, composed chiefiy of (juartz and orthoclase^
together with, usually, a small proportion of plagioclase. (Plate II,
Fig. ;3). Miciocline though sometimes present is of rarer occurrence.
These pebbles are embedded in a much finer groundmass relatively in-
significant in quantity, originally felspathic, but which is now composed
of a confused aggregate of minute scales of yellowish-gre. sericite
arising from its decomposition. A large amount of chlorite is present
usually disseminated in irregular shreds and fragments, althougli some-
times also forming part of the finer interstitial material, while the abun-
dance of this mineral gives the prevailing greenish tint to the rock.
Epidote and zoisite are also commonly abundant, and occasionally
calcite, all these representing secondary products of alteration. Pyrite,
magnetite and ilmenite are also very common constituents, the last
mentioned mineral usually showing somewhat advanced alteration to
leucoxene. Zircon, sphene, apatite and brownish dichroic touimaline,
likewise occur, but are not by any means abundantly represented.

(JKOI.OdKAr. SlUVKY OK (.'AXADA,

Vol,. X.. I'AllT I., I'r.ATK II.

Vu:. 1.

Fi(i. 3.

Fui. 4.

Vu,. 1. Micropuikilitic stnictmi' in lioiiil)!i.n(lc of dioiitc West Ann, Liikt- Nipis'^iiiK'. X <>.").

Vu:. 2. — I'riniury cpidiitf in l)i(itit(' of i|ii!irt/.-niica-tii()riti'-t,'n»Ms.s— Cordon Cirfk. tiim mill's troin
Ldus; Sanlt, Lake 'rcniisciuiing. X ''••">.

Kk;. 3.— Charni'tfr and position of in IikIimI fra^jnicnts in typical ^jrcywacki'— Little Kivir, Lakr
Tt'iiiiscaining. X <J'>.

Fiti. 4.— Kim of c'liliiritc, siirnmndinj,' an^jite of diabast — Fanny Lake. X •">-■

■i.1

BARLOW

time (

bands

as it I]

colour

duced

ties is

east CO

Bay ail

altliouf

Tii(' col

to the (

atlditioi

striped

foruiinsr

ful mosf

are esse

finer sta

dence of

in places

some of

siurgest c

in some i

The St

usually, t

The comp

coinpacte(

the produ<

leucoxene

rock in t

arranged i

or areas.

The mici

tion of th

The lighter

less proport

incipient se

represented

show a prep

what exten;

the prevailir

MRLOW

]

nURONIAN.

101 I

In ascending, this rock gradually becomes finer grained, at the same Slatp or slaty
time developing a marked slaty structure parallel to certain colour ^ ^'
bands which represent original bedding. This slate, or slaty grey wacke
as it may be called, (foi- in places large masses though exhibiting the
colour striping are altogether devoid of any structure except that pro-
duced by jointing), varies greatly in thickness, and in occasional locali-
ties is not represented at all. The high hills found on the north-
east corner of High Rock Island, as well as on the west side of Cross
Bii}' and Sandy Inlet, lihow sections over a hundred feet in thickness,
although in most cases the rock does not occur in such large volume,
Tho colours occur in alternating bands showing a gradation from one
to the other; usually of different shades of green with sometimes the
addition of reddish-brown and black, thus producing a very beautiful
striped rock. In some instances certain beds have been broken up, Autoclastic
forming an autoclastic icjk, which, when recemented, exhibits a beauti-
ful mosaic of irregular though angular fragments. The constituents
are essentially the same as described above, diflfcring only in their
finer state ol: division. The fragments as a rule show little or no evi-
dence of water-action, l)eing irregular and sharply angular in outline)
in })laces forming an intorlocking mosaic of quartz and felspar grains,
some of which have evidently originated in situ, while other portions
suggest considerable recrystallization which has certainly taken place
in some instances.

The structure in occasional instances is that of a microgranite, but Microscopic
usually, the clastic origin is at once brought out by the microscope. ^[.^",^ ""^"
The component fragments are remarkably uniform in size and closely
compacted together, with little or no finer interstitial material, while
the products of decomposition such as chlorite, epidote. sericite and
leucoxene are partially scattered, somewhat promiscuously, through the
rock in the form of irregular grains and scales, while many are
arranged in a more or less definite manner in irregularly curving lines
or areas.

The microscope reveals at once the nature and difference in composi- C'onqiotiition
tion of the colour-bands that so frequently characterize the rock. " '* '^^
The lighter green bands show a prevalence of quartz together with a
less proportion of felspar, the latter being either fresh or showing only
incipient sericitzation, while chlorite and iron ore are only sparingly
represented, if at all. The darker green bands, on the other hand ]';.\iilanatiou
show a preponderance of felspar, much of whiv.h has undergone some- Viamis.'"^
what extensive saussuritization, which, together with chlorite, gives
the prevailing darker green shade to this portion of the rock. The

il^j

liil

il'

I !

102 I

NIPIS8IN0 AND TEMISCAMING REGION.

f^iiartzite
grit or arkorio,

dark, almost black, Hues or stripings are seen to be composed of an infi-
nite number of small crystals and opatjue particles of magnetite,
together with a much larger proportion of ihnenite, which, despite its
extensive alteration to leucoxeue retains much of its original dark
colour and opacity. The reddish-brown stripes are highly fclspathic in
composition and owe their colour to abundant disseminated hydrated
peroxide of iron. These slates evidently in most cases represent the
consolidation of what must once have been extensive beds of volcanic
mud or ashes. In certain instances, as on the eastern shores of Lady
Evelyn Lake and on Turner Lake, they merge into coaiser grained
irregular banded or foliated tufaceous rocks, which occur in immediate
juxtaposition with large plutonic masses, while in other cases, as on
the east shore of Lake Temiscaming, to the north of Wright's mine,
they are interbedded with coarse volcanic breccias or agglomerates
made up of diabasic and quartz-felspathic fragments embedded in a
paste composed largely of chlorite.

In ascending, this rock gradually becomes much coarser in grain,
finally passing into a quartzo-felspathic sandstone, although in certain
places the latter rock was occasionally met with resting directly upon
and merging downward into a basement composed of red granitite.
This arkose is usually rather coarse in texture, in most places showing
the characters of a grit, while certain bands or portions are conglome-
Dcscription of ratio. iLany of the larger fragments in the conglomeratic phase of this
rock represent very distinctly rounded or waterworn pebbles, the
largest of which vary from an inch to two inches in diameter. These
are composed, for the most part, of grayish-white, translucent, often
much fractured quartz, and many of them are surrounded by a thin film
of oxide of iron. Occasionally some pebbles of red quartz are present,
and still more rarely others repiesenting a " stretched " felspathic
quartzite. I3esidt'S these there are greenish, grayish and pale-brown-
ish, usually angular, or at most subangular fragments of an extremely
fine-grained rock, seemingly identical in compo ition to many of the
chalcedonic-like fragments embedded in the vitrophyre tuff described
bj' the late Prof. G. II. Williams from Onaping, Ont.* Besides these
there are small, often angular fi-agments of red and yellow jasper
together with smaller pieces of both reddish and grayish felspar.
These are embedded in a matrix composed largely of yellowish-green
sericite, which, on account of its relative abundance gives the prevailing
tint to the whole rock. Tiie rock, as has been stated, represents almost
altogether the consolidation of true dotrital material derived from the

*Anmuil Kt'iH'rt, <^}pol. Surv. Can., vol. V. (N.^.), Part I, IHIK) !)1, (). 74k. Sections
Nob. 35 and 42.

frupnonts.

Composition
of arkose.

■]

IIUUONIAN.

i03 I

Scvt'ral
varieties of
arkose.

breaking down of granite, a portion of which is represented by expo-
sures covering an area of nearly six square miles in the vicinity of the
Old Fort Narrows on Lake Teiniscaniing, although some of the eiubed-
deil fragments are rather typical of volcanic ejectamenta ; thus evidenc-
ing the continuance of the explosive activity, though with much dimin-
ished violence, which characterized the earlier portion of the Huronian
period. The nature and detailed description of the passage of the
biotite-granite into this overlying arkose, is fully discussed in the geo-
logical description of the exposures encountered on the shores of the
northern part of Lake Temiscaming.

The least altered form of this rock is a rather coarse arkose, which
upon a superticial examination bears a remarkably close resemblance
to an ordinary irruptive-granite. The constituent grains, mostly an-
gular in outline, consist of quartz, orthoclase, plagioclase and microcline,
somewhat closely compacted together, with a very little intervening
finer felspathic material which is undergoing decomposition to kaolin
and sericite. The reddisl) colour is imparted to the rock as a result of
tlie abundance of ferric hydroxide which fills not only the minute Jis-
sures but also stains the larger felspathic individuals. Other varieties
which show no great degree of alteration or attrition and assortment
through aqueous agencies, are distinguished macroscopicaliy by being
brownish, pale-pinkish or grayish in colour.

A rather typical specimen of the prevailing greenish variety or "sea
green quartzite" as it has been called, obtained from a point on the
east side of Lake Temiscaming (Boat-field Point) about half a mile east
of the Hudson's Bay Co.'sold post, shows the rock under the microscope
to have originally been composed of felspar and quartz. The quartz is Comiwsition
in clear colourless fragments, sometimes with tolerably even outlines, of iirkose on
but usually presenting very irregular ones, and the larger fragments Temiscaminfr
are often made up of several interlocking grains. The felspar which
was originally present, is now almost altogether converted into pale
yellowish-giei n sericite which gives to the rock its prevailing colour.
The sericite scales are usually exceedingly minute but occasionally
their presence can be detected macroscopicaliy. There can be little
doubt that much at least of the felspar has been altered in situ. This
alteration of the felspar to sericite is shown in a beautiful manner in
the section. It has l<?ft very irregularly shaped cores in the centre of
the felspar individuals. The field evidence shows in the iiost positive
manner that the rock has had a clastic origin, but the materials, which
nmst have originated in the immediate vicinity, show but slight
evidence of having been waterworn.

' ■'(

■MP J

■ AW

111 I

White
quart.'.iU;.

■!

\i: ,'

I i I

■

TliickneifH of
} [uroniaii.

Diabase and
gabbro.

101 I

Maprmat'c
(liffereiitiatiuii

NIPISSlNf! A\D TEMISCAMING REGIOX.

At ths very summit, in occasional localities, (as on the west side of
the north arin of Nonwakamiiig Lake as well as near High Pond on
Maple Mauntain to the west of I/i ly Evelyn Lake), this reddish or
greenish arkose is overlain by thick massive beds of whitish or grayish-
white quirtzite. This rock is made up of angular or subangular frag-
ments of ordinary j^ranitic quartz filled with the usual inclusion-, embed-
ded in a finer mosaic composed of quartz fragments together with
soricite. It is often much shattered and slieared, the sericite present
(and which is most abundant along th'^ planes of pressure-cleavage)
being the result of izitense dynamic action on the felspar originally pre-
sent. This arkose, forming the topmost member of the ITuronian in
this district, varies greatly in tliickness. In the vicinity of Lake
Temiscaming, hills composed of approximately horizontal strata of this
rock rise to a height of live hundred feet above the lake, while to tlie
west of Lady Evelyn Lake and forming the bulk of Maple Mountain,
the total thickness represented is nearly eleven hundred feet.

The greatest total thickness attained by the Huronian formation in
this district is nearly eighteen hundred feet, made up roughly as fol-
lows : — (1.) Breccia-conglomerate GOO feet. (2.) Slates and slaty grey-
wackus 100 feet. (3 ) Quartzite grit or arkose 1100 feet.

Diabase and Gabhro,

Massive rocks of both the diabasic and gabbro types are frequently
and intimately associated with both the epiclastic and pyroclastic rocks
of the Huronian. iSuch rocks have often, in fact, been included as
part of the Huronian system, although they appear indeed to be
practically contemporaneous in origin in many cases, but they should
not be counted as a part of the system when its thickness is to be
ascertained. These l)asic intrusives apparently represent the deeper
seated pi utonic action, connected with the volcanic outbursts that gave
rise to the ejectamenta wliich are so abundantly represented.

Many of the masses of this kind are intimately associated with, and
lerge gridually into, a rather typical (lesh-red biotite-granite or
-ranitite, while several of the exposures are pierced and traversed by
irregular dyke-like forms and masses of pegmatitic material. This
gradual passage into granitite can be directly and continuously traced
in a number of instances in single outcrops. The most reasonable
assumption is that all three rock -species, dialjase, gabbro and granitite
represent highly differentiated portions of the same magma which have
solidified at temperatures corresponding with their composition.

IIIHONIAN.

105 1

These basic plutonic rocks cliiiracterize large areas, occurring for Oceuirenct'Hof
the most part as a series of irregular, though often somewhat rounded i^'^^k^.'' "'""'"
batholitic masses, which send off large arms or dykes to intersect the
neighbouring stratifi* d rocks. In certain localities, as on the south-
west side of Kound Lake (Wawiagama) a little beyond the western
limit of the Lake Temiscaniing sheet, as well as at Beaver ]Mountain,
south of the mouth of the Montreal lliver, they appear to represent
the consolidation of what may possibly have been intruded sheets or
sills of molten material. Tlu.><, however, could not be positively ascer-
tained, as the covering of clastic rocks, if originally present, has been
removed by subsequent denudation.

These rocks, in the area here considered, uuially possess a medium
texture, although in many instances they are so coarsely crystalline that
most of the principal constituents are plainly apparent. In general
they vary from greenish -gray, through dark-green to almost black in
colour, although in many of the coarser phases the prevalence of felspar
with a distinct flesh-red colour, gives a prevailing reddish tint to
the whole mass. In most places they have a massive much jointed
character, and this, together with the extensive shearing action to
which these rocks have been subjected, makes it exceedingly dithcult
to secure even a hand specimen of well shaped outline. In occasional Basaltic
localities, as at Manitou Rock on the west side of Lake Temiscaming, «tnict\ire.
the rock shows a rude columnar or basaltic structure.

Under the microscope, these rocks present a remarkably uniform
inineralogical composition in the several separated masses, while the
specimens obtained almost invariably exhibit, in a very typical manner,
the ophitic structure which belongs essentially to diabnse, although in
some other areas, as well as in certain portions of the same mass, it
sometimes shows the holocrystalllne or granitoid structure of gabbro.

The least altered variety of the rocks of this class, is made up Com position
essentially, and almost wholly of phigioclase and augite, the former '^'^ ''.'"''"*''''*""
mineral being present in the usual idiomorphic lath-shaped individuals
penetrating the allotriomorphic augite. From the extinction-angles,
the plagioclase is near the basic end of the series — labradorite and
bytownite. The mineral is sometimes rather fresh and glassy, although
frequently it shows a marked turbidity, owing to the development
in it of the usual saussuritic products of decomposition, while the
augite, which when fresh is of a distinct reddish-brown colour, is
as a rule partially decomposed to green trichroic hornblende. A few
rather broad tabular unstriated individuals of felspar are usually
present, and may possibly represent orthoclase. lleddish-brown,

lilt!:

V>\ \

;. I

106 I

NIPISSINO AND TEMISCAMINO REGION.

ill

■1

Diabase of
(^uinii Point.

(i.ibbro of
Houth-west
arm of Lake
Tcmagaini.

strongly pleochroic biotite is found in irregular plate.«, but not in any
excessive amount. Quartz is likewise a rather cdnstant constituent,
occurring in small clear irregular areas filling in the lesser interspaces
between the felspar and augite. The ilmonite present very often
shows the characteristic "gridiron" alteration to leucoxene. In cer-
tain instances, as at Quinn Point on the east side of Lake Temisca-
ming, the rock has unflergone considerable decomposition, the augite
being completely altered to green trichroic hornblende (uralite.)

Most of this uralite is the usual compact dark-green variety, but
some of it has assumed the actinolitic habit. In other localities, as oa
the Quinze liiver, the diabase has undergone still more advanced alte-
ration, the whole rock-mass being converted into a rather typical
hornblende-schist or amphibolite as a result of intense pressure. Tra-
ces of an ophitic structure still remain, showing clearly the original
character of the rock, altliough in places this is masked by the extreme
deformation to which the rock has been subjected. The process of the
uralitization and decomposition of the augite is very interesting and
instructive, showing first an alteration to the compact green ti'ichroic
variety of hornblende, the indiviu'^als presenting deep-coloured bor-
ders with pale interiors. This, with an increase in deformation, assu-
mes the fibrous or actinolitic habit, which, in turn, is decomposed to
chlorite, the individuals of the last-mentioned mineral retaining much
of the marked pleochroism of the hornblende. Some of the plagioclase
seems remarkably fresh, although the greater proportion is altei'cd to
opaque greyish masses of saussurite, the resulting epidote, zoisite and
sericite being especially al)undant in those portions of the rock which
have yielded most to pressure. The ilmenite originally present, is often
almost wholly converted to a brownish sphene wliich occurs in grains
or aggregates scattered through the rock.

A section prepared from a specimen representative of a small mass
of highly altered gabbro that protrudes through the breceia-con-
glomerates and slaty greywacke on the east shore of the south-west
arm of Fjake Temagami, shows that the rock is now composed of fel-
spar, quartz, pa'e-green fibrous chlorite, biotite and zoisite. The
mutual reactior. of the felspathic and feiro-magnesian constituents has
been so pronounced, and the resulting decomposition products have in
many cases wandered so far from their former positions, that the ori-
ginal structure is to a certain extent masked. Zoisite is a very abund-
ant constituent of the rock as an alteration product, occurring in irre-
gular grains and crystals. Sphene is also quite abundant and has
resulted from the decomposition of ilmenite originally present. Small

•AHUM)

cores of
brownis

The 1
Beaver
designat
ture is v
planes o
greenish
scope, tli(
The plagi
of the s(
of the im
position
presence c
site result
augite is a
the laths r
variety fie
are characi
(schilleriza
ent alterati
able quanti
scales. A
opaque iron
grains tliroi
irregular ai
pentinuous
dotted with
dote, the wl
ii-regular ma
in serpen tin(
small residue
refraction th

Besides th(
ciated with ti
trusives incot
clearly do not
have been pre
ration than tl
tive statemeni
conjunction h

nUHONIAK.

107 I

cores of the unaltered ilmenito .still renmin. The biotite is of a pale-
brownish colour as a result of the leaching out of a portion of its iron.

The rock composing the upper and more precipitous portion of Diabase of
Beaver .Mountain, or the "King of the Beaverh" as it is sometimes \i,'„„,taiii.
designated, is a dark greenish-gray diabase, in wliich the ophitic struc-
ture is visible to the naked eye. It is much sheared and broken, the
planes of cleavage and jointing being plentifully coated with dark-
greenish minerals belonging to the chlorite group. Under the micro-
scope, the rock is seen to be composed mainly of plagioclase and augite.
The plagioclase, which from the extinction-angles is near the basic end
of the series (probably bytownite), is usually pretty fresh, but some
of the individuals are rather turbid, owing to the presence of decon'-
position products, while considerable areas are characterized by the
presence of light-greenish sericite and yellowish-green epidote and zoi-
site resulting from tiie saussuritization of the felspar substance. The
augite is as a rule fresh and occurs in allotroraorphic masses pierccl Ly
the laths of plagioclase. It is reddish-brown in transijiiuced light, a
variety fiecjuently met with in diabases, and many of the individuals
are characterized by the presence of innumerable rod-like interpositions
(schillerization products.) Frequently it is noticed untlergoing incipi-
ent alteration to compact pale-green trichroic hornblende. A consider-
able quantity of reddish-brown biotite is present in irregular plates and
scales. A little qucartz was also noticed, while both pyrite and an
opaque iron ore, probably ilmenite, are present, scattered in irregular
grains throughout the section. Besides these, comparatively large and
irregular areas may be seen composed of a pale yellowish-green ser-
pentinuous substance, associated with secondary caleite and often
dotted with strongly refracting grains and elongated fragments of epi-
dote, the whole showing aggregate polarization. Very oiten these
irregular masses show the characteristic net-like structure so common
in serpentine derived from the decomposition of olivine, altliough the
small residual cores still remaining, in some cases have a lower double
refraction than is usual in this mineral.

Besides the masses above referred to, which ire so intimately asso-
ciated with the elastics of the Huronian, there are also similar basic in- nuAc intru-
trusives incorporated with the Laurentian gneisses and granites, which re,)^';^^'," "
clearly do not belong to the same magma from which these latter rocks
have been produced, In most cases these appear to be of earlier gene-
ration than those associated svith the Huronian, although no very posi-
tive statement can be made on tliis point. The gneiss in immediate
conjunction is often more basic and hornblendic, seemingly showing

•• I,

^ 1

■

J 3

; ii

^ !»

[

i;]

Diabase of

Expectatioii

Lake.

Adjacent
rock.

108 I

NIPI.SSIXO AXn TEMISCAMING REGION.

a commingling l)y actual fusion of the two rocks along their line of
junction.

Outcrops of a uralitic diabase marking the occurrence of a small
urea of this rock, were noticed apparently cutting and altering thegra-
iiitite-gneiss exposed on t!ie north-west shore of E.'cpectation Lake
near the south-west end. The diabase is much finer grained near the
junction with the gneiss. The specimen obtained showed the rock to
be a medium-gniined, dark-green, basic eruptive, the diabasic structure
of which can be seen in the hand specimens. The microscope shows
it to be a remarkably good instance of a diabase in which the bisilica-
tes have been almost entirely decomposed, while the plagioclase remains
in a comparatively fresh, unaltered condition. The minerals now pre-
sent are plagioclase, hornblende and chlorite (doubtless representing
augite originally present) ilmenite accompanied by leucoxene, apatite
and sericite. A few of the plates of chlorite look as if they may have
been derived from biotite. The plagioclase is in rather broad lath-
shaped .sections whicii interlace, giving a coarse ophitic structure
to the rock. It is well striated (both alhite and periclino laws being
represented) possesses \ery uneven extinction and has evidently been
suiijected to a coii'-i lerable degree of pressure, many of the crystals
being shattered. The augite originally present is now almost entirely
altered to a pale yellowish-green chlorite. It has evidently passed
through an intermediate st i;e of alteration to hornblende, as that
mineral, of a pale bluish-green colour and librou-f, in which the altera-
tion to chlorite is so far advanced as to almost entirely obliterate the
optical characters of the hornblende, surrounds lighter, still more
alterel cores which douljtless represent the original augite. Magnetite
result' ig from the decomposition of the bisilicates, a little apatite,
sericite and epidote occur as secondary products.

This diabase is in contact with a dark green, fin?-grained, compact,
foliated rock, sprinkled with little crystals of pyrite. Under the micro-
scope, the ground mass consists of a fine-grained mosaic of clear quartz
and felspar, through which run little strings of a brown biotite, in fine
brightly polarizing scales which are evidently of a secondary origin, and
in places show an alteration to chlorite. Throughout this fine-grained
material, larger grains of quartz and felspar (principally microeli^)
are distributed, which by their granulated appearance and very uneven
extinction bear unmistakable evidence of the dynamic action to which
the rock has been subjected. Large irregular grains of pleochroic
epidote, colourless to pale yellow, frequently showing good cleavage,
are abundant, as are also large clove-brown crystals of sphene. Crys-

■ARLOW.

HURONIAN.

109 I

tals of zircon, fairly large, and frequently showing marked zonal
structure are plentiful. Some pyrite and iron ore were also observed.

Another niiiss of these b.asic eruptivcs that may he mentioned in Basiu
this connection, is woll expose'! on tlie shores of McDiariuid Lake, the .Mciiiarmid
southern part of Breadalbane Lake and the isUiniis and points chiefly I"»l<'-
in the central portion of Fanny Lake.

The rock is dark-creen, almost black in colour, weathering rusty '•"><>»•
or brownish owing to the oxichitinn ot the large amount ot jiynte
finely disseminated through it. Atmospheric agencies have likewise
produced a rough, though somewhat finely pitted surface, owing to the
decomposition and removal chiefly of the coloured constituents, leaving
a reticulated surface formed by the felspar standing out in
relief. The relations with the surrounding gneissic rocks of the Lau-
rentian series seem to show its earlier genesis, and these foliated and
much more acid rocks are rendered relatively more basic or hornbleudic
in the immediate vicinity of the line of junction, apparently as a result
of the free interchange, through actual fusion, of the material of both
rocks. The basic rock has usually a rather well miuked foliation,
which corresponds in general with the strike of the inclosing ,<;neissic
rocks. On McDiarmid Lake this strike is 8. L't° E., tlie rock being
nearly if not quite vertical, while on Fanny Lake the strike is X. 35°
E. with a dip to the north-west of 85°.

Under the microscope, this rock is seen to be a rather fre>h diabase Micki^oI'ic
. . structures. ;

composed chiefl}' of plagioclase and augite. The plagioclase is unusually
fresh and glassy, and well striated, both aibite and i)ericline laws being
represented. It occurs for the most part in ratlier broad, lath-shaped
crystals penetrating the irregular individuals of aus'ite. As a result
of pressure, it usually exhibits a wavy extinction, is sometimes bent or
curved and occasionally fractured and dislocated. The augite is
of the reddish colour so often noticed in diabase and occurs in irregular
polysomatic areas. These composite individuals or masses are sur-
rounded by a narrow rim, of remarkably uniform width, composed of
fibrous and I'adiating scales of pale-greenish chlorite, each separate
scale being approximately at right angles to the outline of the unal-
tered portion. (See plate IL, fig. 1.)

The augite is rather frei?h, while the line of division between these
"reaction-rims" and the unaltered portion of the individual is very
sharp and abrupt. Associated with the augite and freciuently com-
pletely inclosed by it are irregular plates and scales of a reddish-brown
strongly pleochroic biotite. Sometimes it is considerably bleached
while occasionally it is altered to chlorite.

'Annual Report, Geol. Surv. Can., vol. I. (N. S.), 188788, p. 155 v.

! !!il':

110 I

NIPISSINQ AND TEMIHCAMINC RK(ilON.

. ' t

Ba8ic- rooks On tho west side of Lnko TemiscuiiiiiiL; nearly fjpposite Lalours

"ni '^'^ """ ^li"*^) l>l!it'k, irregular, rou<,'lily weathering masses of a very liasic rock

may Ijc noticed cauglit up in and penetrated by the assoiiat«!d graiii-

tite-gneisses mapped as Laurentiun.

The liand-spccimen examined is black in colour with glistening
scales of mica abundantly developed through tin; mass. The weathered
surface is rough and pitted, resembling a pumice-stone. I'nder the
microscope, the component minerals are seen to be hornblende, l)iotite
plagioclase, garnet and iron ore. The hornblende is green in colour,
trichroic, and occurs in large areas composed of an aggregate of suwill
individuals. Occasiunally these aggregates show a pale inteiior with
a dark-green bordtir surrounding the nuisses, !t is undoubtedly sec-
ondary in origin and .some of it isactinolitic, and is the most abundant
mineral in the section. The biotite is rather pale in colour owing to
the removal of a part of the iron, and freipiently shows pleochroic
halos surrounding embedded fragments of the other constituents of the
rock. The plagioclase is not nearly so abundant, and is very f recpienlly
almost opiujue, from the inclusion of dark-brownish dust like particles.
The gainet is in irregular grains as is also the iron ore, which is prob-
ably magnetite. A some.vhat rude ophitic structure can still be
detected in the rock.

Occurrence of Besides the foliated diorites that occur as integral and extremely
dioritcs. basic portion of the prevailing Laurention gneisses, there aie occasional

and comparatively large irregular areas of massive diorite, which are
apparently of earlier genesis than the foliated rocks with which they
are associated. One of the largest of these masses noticed, occurs on
the southern mountains to the south-west of the west point of Maski-
On Bear Bay. nonge Island, on Bijar Bay in Lake Nipissing. The mass has, roughly
speaking, a diameter of a little over four hundred feet. A border of
black mica-schist (probably a mica-diorite-gneiss) nearly three feet in
width, separates this massive basic rock from the gneiss, the foliation of
the diorite gneiss curving lound the outline of the mass. The whole
mass is penetrated by reddish quartzo-felspathic masses and dykes which
are evidently extremely acidic portions of the same magma from
which the gneisses have solidified. Fragments of the basic hornblen-
dic rock are embedded in gneisses near the line of junction.

Microscopic
character.

Under the microscope, this rock is seen to be a garnetiferous granite,
being composed of plagioclase, orthoclase, quartz, hornblende, an ortho-
rhombic pyroxene and garnet with smaller quantities of sphene and
iron ore. It possesses a holocrystalline structure and shows only slight
evidences of pressure in the uneven extinction of the quartz and felspar

■ARLOW

individii;
is usua!l\
pleocliroi
Excellcti

a. H. \\-

occupiecl

crowded

ence to oi

complete

structure,

interpene

The ort
parallel c
roism, wit'
ant and ov
usually in
luby-rcd ii
irregular g
iron ore is

The rock

most part, i

classificatioi

are to be fo

lakes formii

across these

give a very

these separa:

coarsely eryj

distinguish;) 1

very massivi

foliated text

tSpawning an

this rock pres

crysts being

felspathic gi

Orthoclase is

inicrocline an^

while quartz,

* Journal of G,

(iHANlTK.

Ill I

■ ^ '\

individiiuls. The felspars as a rule are quite fresli. Tlie horriblondf
is usually in massive irre_'ulai- indivitluals (if a {jrccii colour and stioiiKly
plcocliioic. t)ccasional individuals siiow f,'o()d ci ystaliui^'raphic outline
Kxcelh'rit examples of tlio niicropoikilitic siiut'ture described by Dr.
G. II. Williauis * were observed. Thus certain nrcus of the rock are
occupied by cumparativcly lar},'o individuals of hornblende which aro
crowded with irregular /^nains of (piart/ arran^^ed without any refei-
ence to one another or to tin* matrix, and, which neithei- possess tin*
complete independence of optical orientation characteristic of granular
structure, nor the entire continuity of the separated portions of two
interpenetratingciystal individuals.

The oi'tliorliombi'-" pyroxene, which is probaV.ly hyjiersthene, has a
parallel extinction, is rathei" liidit in colour and has a feeblt^ pleoch-
roism, with light-yellowish to pale reddish tints. It is somewhat abund-
ant and occurs in individuals having ii regular outlines. The garnet is
usually in large individuals full of irregular ciacks. It is pale
ruby-red in colour with characteristic high relief. The sphene is in
irregular grains frecjueiitly imbedded in the hornblende. An opaque
iron ore is rather abundant in the section examined.

OR.XNITE.

The I'ock to which this general name has been applied, is, for the fj i
most part, a biotite-granite or granitite according to Kosenbuch's ^','
classificati(m. As the details of the numerous exposures of this rock
are to be found in connection with the geological de.scription of the
lakes forming the series of canoe-routes which atlbrd an access to or
across these mas.^es, it will only be necessary, in this connection, to
give a very geneial notice of this rock, applicable alike to most of
these separate occurrences. It is of a prevailing reddish colour, rather
coarsely crystalline, the principal constituents being usually readily
distinguish.ible with the unaided eye. In some localities it presents a
very massive structure, while occasionally it shows a very distinct
foliated texture. In several cases, notably in the area adjoining
Spawning and Young Loon bays of Lake Temagami, occurrences of
this rock present a very coarse, often porphyritic, variety, the pheno-
crysts being Carlsbad twins of orthoclase developed in a quartzo.
felspathic ground-mass rather poor in ferro-magnesian material,
Orthoclase is the most abundant felspathic constituent, although
microcline and plagioclase are both present in considerable quantity,
while quartz, which is as a rule proportionately less in amount than

•Journal of Geology, Chicago, vol. I., No. 2.

i.i'. tir (if
^riMiiites.

■; L

112 I

NIPlHSINfJ AND TKMISCAMINd RKfilON.

■aRloa

1 It

1^ I

<tr»'enKtono
iniiNNi's in
tp-imil" M.

Fiatcr
t'luptivc

Dykes near
Les Erables.

Microscopic
character.

the felspar, is of the prevaiiini,' f,M{initio viiiii'ty full <i j^lass and other
inclusions. The coloured constituent is jL^enenilly hiotite which has
either partially or wholly been doconi})osed to a paie^reenish chlorite,
the individuals preserving nuich <if the original marked plcochroisin of
the niinor.U from wliioh it has been derived. Epidoto and sphene are
both very alnmdant anil freijuently in such largo crystals and fray-
ments as to bo niacroscopically discernable.

In the midst of all the large granite areas, considerable tracts are
characterized by greenstone, while masses of this greenstone (diaba.se and
gabbro) are froi|uently ,so intimately associated with the granite that
separation, especially on the scale aiUtpted on the accompanying maps,
woukl be imp"ssible. Dykes and masses of granite and pegmatite
likewise accompany outcrops marking the largo occurrences of diabase
and gabbro. Although in most cases c'l marked and sharp contrast
e.vists between the two types of rocks (acidic and basic), it was
rather definitely ascertained that the njcks are very intimately related,
and it seems quite evident that the dates of their respective intrusions
are nearly synchronous, the basic t}'pes representing the first segre-
gations of a magma which ultimately crystallized as granitite and
granitite-pegmatite. On the other hand, these areas of massive
granitite merge into foliateil granites or gneisses which are usually
indistinguishable from, and sometimes co-extensive with similar
material described and mapped as Laurentian.

POST-ARCII.KAN KUUPTIVES.

Besides the huge masses of diabase and gabbro that are so
intimately associated with the Laurentian and Huronian, most of
which seems to be practically contemporaneous with these rocks, there
are other intrusives occurring principally in the form of dykes, which
cut the Laurentian gneisses, and are thus very obviously of Uiter origin.
The greater number of these occurrences possess sharply defined and
appi'oximately parallel inclosing walls, although some have filled irreg-
ular cavities of the pre-existing rocks, and thus possess uiort, ill-defined
contours.

The first of these which may be mentioned, was noticed on the east
side of the Ottawa River between Les Erables Rapids and Snake
Creek, the intrusive masses apparently piercing the associated granitite-
gneisses. Macrosoopically, the specimen examined shows a very coarse-
grained dark-gray rock, with a reddish tinge given by the abundant
presence of a wine-coloured almandine garnet. Under the microscope,
the rock is evidently a very typical example of crushed and epigenized

gabbri
are plajj
hornble
serpenti
tion.
present,
of the SI
uneven
is quite
spaces ir
ment of
kaolin
selves in
shows a
greenish
almost iso
almost in
particles,
products n
such impu
Some of th
pentine. 1
the most pi
ing from tl
which, toge
by the perc
crystals an(
area surroui
in comparat
strongly ple(

On Iron j

sected by 1;

micaceous t

these occurn

rock to vary

with a distin

in crystals is

are much co

and lacking

material. Tl

decomposed a

with acid. 1

•ANIOA

]

POST-AKCn.SAN EKUPTIVE8.

113 I

gabbro. Tho minerals noticed as present in the microscopic section Dotaila of
are plagioclase, unstriated felspar (possibly orthoclase), (quartz, diallage ■*'*''"=^'"'''-
hornblende, biotite, garnet, apatite, iron ore, pyrite, together with
serpentine and chlorite occurring as secondary products of decomposi-
tion. The plagioclase, which is by far the most abundant felspar
present, is much disturbed, bent and occasionally broken, while many
of the surviving large individuals show in a very beautiful manner the
uneven or undulous extinction due to pressure. Much of this mineral
is (juite fresh and glassy, although many irregular and often large
spaces in the crystals are very turbid, owing to the abundant ilevelop-
ment of exceedingly numerous and minute scales of sericite and
kaolin ; these products of decomposition sometimes arranging them-
selves in plumose aggregates. The diallage, when free from impurities,
shows a rather faint, though perfectly distinct pleochroism, from light-
greenish to pale-reddish. Many of the larger individuals are rendered
almost isotropic by the interposition, along the planes of parting, of an
almost infinite number of mi; ttd brownish, more or less opaque
particles. All stages in the development of these schillerization
products may be noticed, from individuals that are entirely free from
such impurities to others which are perfectly crowded with them.
Some of the diallage shows somewhat advanced decomposition to ser-
pentine. The brownish-green trichroic, hornblende present, occurs for
the most part in the form of " reaction rims " surrounding and result-
ing from the alteration of the diallage. The wine-coloured garnets,
which, together with the colouring of the diallage, have been developed
by the percolation of heated vater (epigenetic action) occur in small
crystals and crystalline fragments, often forming an irregular zona]
area surrounding the bisilicate material. The biotite, which is present
in comparatively small quantity, is of a deep reddish-brown colour and
strongly pleochroic.

On Iron Island, in Lake Nipissing, the prevailing gneiss is inter- Eruptive
sected by huge irregular masses of a dark brownish-gray highly i"ouTsland
micaceous trap. The specimens secured as illustrative of one of
these occurrences near the south-west point of the island, show the
rock to vary considerably in texture, some portions being fine-grained
with a distinct approach to porphyritic st-ucture, the biotite occurring
in crystals with sharply defined hexagonal outlines ; other specimens
are much coarser grained, with the biotite in broad irregular flakes,
and lacking the distinct porphyritic appearance of the fine-grained
material. The rock weathers to a rusty brown colour, is greatly
decomposed and filled with carbonates, causing it to effervesce freely
with acid. The microscope shows that the principal minerals now
8

■ t :

: !

ii:;i

m ■
.1

8 iij

III

it !

I if

■i :i

!
i 1 1

Microscopic
character.

Dvk(f8 on

Manitou

Islands.

Microsc()i>ic
.structure.

lU I

NIPIS81NG AND TEMISCAMING REGION.

present are l)iotite and gfirnet, with abundant iron ore, some acces.sory
augite, a little hornblende (?) and nm8.se3 of calcite, etc., which may
represent in part felspars originally present, though none are now observ-
able. Apatite is abundant in good-sized long prismatic crystals. The
section of the tiner-grained portion contained no garnet, while in the
coarse-grained phase of the rock this mineral is exceedingly abundant.
The garnet is of a peculiar yellowish-brown colour and re.senibles the
melanite variety, while the coarse portion of the rock might be described
as composed es.sentially of biotite and melanite garnet with some little
accessory augite and perhaps hornblende. The rock is a most remark-
able one and further investigation of fresher material might prove it
to be a hitherto unobserved member of the mica-peridotite family.

Another interesting and rather rare species of ^^ke-rock was noticed
on the most southerly of the Manitou Islands in Lake Nipissing.
Near the southern extremity of this small island, dykes as well as
irregular masses of an alnoite-rock cut the dark reddish and greenish
granitite-gneiss representing the Lauren tian. One of these dykes is
about ten feet in width, running in a direction nearly east-and-west
and inter.secting the foliation of the gneiss almost at right angles.

Another occurrence showed a fissure about six inches in width filled
with the same material. Muiray**^ mentions the occurrence of intrusive
masses of the same rock as .seen on one of the islands in East Bay opposite
Callendar station. The specimens of this rock consist of a fine-
grained greenish groundmass in which are embedded large phenociysts
of biotite and augite, together with rounded greenish masses, which at
first sight seem to resemble concretionary or pebble-like inclusions.
On examination, these simulate rude prismatic crystals, but only
the skeleton forms remain, filled with decorapo.sition products, chiefly
calcite, and that may possibly repiesent olivine, originally present. In
the hand-specimens the large plates of biotite and phenocrysts of
a.gite are especially noticeable, at once suggesting its probable close
affinity to the alnoite first described by Tornebohmf, in 1882, from
the island of Alno, in Norway. The thin section, under the micro-
scope, shows an exceedingly fine-grained and decomposed groundmass
consisting of an intricate mixture of brightly polarizing scales of
bleached biotite, chlorite, spicules and crystals of hornblende
(actinolite), calcite, pyrite, iron ore and leucoxene, in which are em-
bedded larger individuals of augite and biotite, the former almost
wholly converted to hornblende and calcite, although the chai-acter-

• Report of Progress, Geol. Surv. Can., lG.53-56p. 122.

t A. E. Toniebohm : Melilit liiwalt friii Alno, (Jeol. Forn. 1 Stoekliolni Fiirli.
1882 p. 240.

■A mow

]

P ST-ARCHiEAN ERUPTIVES.

115 I

istic skeleton forms remain. In this matrix are developed large
though somewhat rude phenocrysts of biotite and augite. The large,
individuals of augite show a perceptible, though somewhat indistinct
pleochroism and are traversed with a network of cracks mort or less
filled with hornblende and calcite, products of its alteration and
decomposition. They are as a rule surrounded by a rim of variable
width composed of the usjual hornblende (uraiite), showing beautiful
deep-bluish polarization colour between crossed nicols. The biotite is
rather fresh, althougU some of the iron has been removed, and, as a
consequence, exhibit brilliant chromatic polarization colour. The
pleochroism, is strong from deep brownish-red to pale-yellow. The
individuals have a hepidiomorphic outline, occurring in elongated
plates and scales which show considerable optical disturbance as ..
result of pressure. The rock doubtless belongs to the group Type of the
which includes the alnoites, monchiquites and fourchites but it is now
so decomposed that its exact position cannot be determiiied. Closely
related rocks have been described by C. H. Smyth, jr.,* from Central
New York, and by Adams, t from Ste. Anne de Bellevue, Quebec, and
from a point on the road between Ashcroft and Savona, British
Columbia, three miles east of Eight-mile Creek.

About five chains north of the last occurrence of this rock, on the j)yko

west side of the same small island, beds of pink crystalline limestone c.""'»S

'_ . . limestone.

occur containing more or less epidote, biotite and hornblende as
impurities. The strike of the rock is abouo N. 80° E., while the
dip is at an angle of 65°. A dyke varying in width from 9i to 1 1
inches, of fine-grained, dark-greenish, almost black rock was noticed
intersecting this limestone in a direction N. 4° W.

Under the microscope the rock is seen to be greatly altered, con- ]\[iL,,.„j.coi)ic
sisting chiefly of microcline and horni)]ende, the latter evidently second- Lluiracter.
ary in origin. The original I'ock, unaltered, was probably an augite-
tuicrocline one and thus allied to the vogesites. The hornblende occurs
in elongated pale yellowish-green individuals considerably altered to
chlorite and frequently forming shc-af-Iike bundles of crystais. A
close study of the section reveals numerous examples of comparatively
unaltered cores of the original augite. The felspar of the rock giving
generally elongated sections appears to be principally microcline,
although some plagioclase wa- also observed. It is turbid, being full of
inclusions of hornblende, sericite, etc Brilliantly polarizing secondary
epidote is abundantly distributed throughout the rock.

•American Journal of Science, April, 1892, August, 1893, and October, 1896.
+ Ibid., April 1892; also Annual Report, Geol. Surv. Can., vol. VII. (N.S.), p.
38811. No. 79a.

fit I

i-\-

i.wgw

il6

NIPISSING AND TEMISCAMING KEGIOX.

li!

Dyke on

Goo8<>

Islands.

Dykes near
Buntiekl.

Siniiku-
(iykcs ni'iir
Sudliury.

Kocks near
Cjillander.

On one of the smaller of the Goose Islands, at the extreme west
end of the group, the pinkish granite-gneiss strikes N. 70° E., with a
dip to the south < 50°. Near the nortli-west end a greenish dyke of
fine-grained material about \\ feet in width, cuts across the whole end
of the island running in a direction N. 58° E.

About three miles and a half north-east of Bontield station (formerly
Callander) a rock-cutting made during the construction of the Canadian
Pacific Railway shows a good section of a massive granitoid gneiss pierced

Fig. 2.

North-east. South-west.

Dykes ok Coxcrktionahy Diahask 3i Milks N. E. ok Bonfikld.

by several dykes of a rusty-weathering medium textured diabase. The
rock has a marked concretionary structure, which is revealed as a result
of ordinary weathering, the successive thin concentric layers of rock
peeling oflf much like the coats of an onion. The dykes cut across the
indistinct foliation of the associated gneissic rocks. Near the walls the
dykes are very much decomposed and schistose, while the gneiss is baked
and altered to a slight degree in the immediate vicinity. The largest
of the dykes, near the south-west end of the cut, is six feet across with
a branching arm about two feet in width. Another dyke near the north-
east end of the outcrop is four feet in width, while the third is only
about one foot in width. The rock composing these intrusions is readily
attacked by atmospheric agencies and is more or less hollowed out
in the adjacent hard gneiss. Dykes and masses of precisely similar
material are exposed along the line of railway between Sudbury and
the Murray mine, which in a thin section under the microscope is
found to be a rather typical and fresh oli vine-diabase. No petro-
graphical examination was however made of the rock from the locality
above described, as the specimens secured were lost in transit.

Along the line of the northern division of the Grand Trunk Railway,
in the vicinity of Callander station to the east of Lake Nipissing, the
various rock-cuttings show good exposures of a mas.sive granitite-gneiss.
As a rule, this is a medium-grained distinctly foliated granitic rock,
in which the dark-coloured irregular strings and layers composed of
the ferromagnesian constituents, (principally biotite), alternate with

BANLAW.

]

POST-ARCH-EAN EUUPTIVES.

t I

Dyke.-i cutting

tlu'Ul.

broader reddish bands of coarse-grained felspar and quartz in which
lie little patches and strings of the darker material. Frequently the
gneiss has a very distinct augen structure, the lenticles composed
almost wholly of reddish felspar being sometimes as tnuch as six inches
in length Vjy two or three in breadth. The strike of the rock varies
from N. 20° W. to N. 20" E. with a prevailing dip to the east at a
high angle, usually over 60'. In some instances the rock is quite mas-
sive, showing little or no evidence of foliation. These reddish grani-
toid rocks are intersected in several places, almost at right angles to
the foliation, by irregular often branching dykes of comparatively line-
grained dark greenish-gray, sometimes almost black rocks. In the
immediate vicinity of the line of contact, the gneiss exhibits a narrow
selvage of much liner grained rock, showing the intrusive action of th»>
dyke, while in some instances fragments of the gneiss have been caught
up and incorporated in the body of the dyke. At the first cutting,
about a quarter of a mile south of Callander, the rock is very massive
and granitoid, but at the second, a well marked foliation has been devel-
oped, running N. 10' W. with an easterly dip at a high angle. This
rock is intersected by two dykes, daik-green to almost black in colour,
containing porphyritically embedded individuals of a black, bright, glist-
ening mineral. The walls of the dykes are more or less irregular, often Hclations of
serrated and frequently presenting re-entering angles of fine-grained \^^ suucfure^
material which penetrates the mass of the neighbouring granitic I'ock.
At the widest places the larger of the two dykes is about seven feet
thick, while the smaller is about two feet. The dyke interrupts the folia
tionof the gneiss and near the contact both rocks are much finer in tex-
ture, while fragments of the gneiss are embedded in the dark-greenish
rock. Under the microscope, the rock possesses a peculiar irregular
granular structure, and the intergrowth of hornblende and felspar gives
to the section a pseudogranophyric appearance. The section is filled with
a dense mass of little shreds of hornblende in a groundmass composed
ohiedy of broad plates of orthoelase. There are numerous large phe-
nocrysts having centres composed of a pale-green diopsedelike pyrox
eue, altered t)n the outside to a green hornblende. Biotite is also
plentiful in large fresh irregular plates full of inclusions. Titanite and
apatite also occur. The whole section is sprinkled with iron ore,
pyrite and granules of epidote. It is a very basic rock, near the syenite
end of the peridotites and between these and the vogesites. It might
be termed a hornblende augite-minette.

The next cutting, situated about A mile south of Callander, runs branching
through a hill of a deep-reddish granititegneiss. At the north end of *'>^''^'''-
the cutting the foliation is quite distinct, this structural feature strik-

llh

<.\

;br

liTW

i :;3:

118 I

NIPIS8ING AND TEMISCAMING REGION.

ing about N. 10^ E. with an easterly dip <t)0°, but towards the
middle of the cutting the rock is very massive, showing only indistinct
foliation. This rock is pierced by irregular dyke-like forms of a
massive, dark, greenish-gray rock, which shows a marked difference
in texture, being fine-grained near the containing walls of the dyke
and coarser toward the middle. There is a selvage of about an inch of
fine-grained granitite near the contact with the darker rock. In some
places these dykes have comparatively regular and straight walls, while
in others they are of somewhat irregular outline. On the west side of

Fig. 3.

Character of
the rock.

West side of cutting, one mile south of Callander, fi.T.R.

SKETCH SHOWING nVKE-LlKK FORMS OK MR'A-PHONOLITE (;i)('rTTIN(! GKAMTK-tiXKISS (b)

the track near the north end, three of the narrower dykes, in approxi-
mately parallel position, cut the granitite and are connected with the
larger and more irregular body of the dyke. The whole section exposed
is a little o\er a hundred feet in length. The finer grained portion of
the dyke, near the walls, shows a very compact dark-green slaty
rock tilled with a multitude of joints, causing the rock to break into a
large number of small, irregular rhombohodral fragments. Under
the microscope it is seen to be much altered and very fine-grained.
It is composed of a groundmass made up of a colourless isotropic
substance, sprinkled all through with irregular patches and spots
(micropoikilitic) of a mineral with higher refraction and very high
double refraction which may be calcite, also occasional laths of a
low double refractive mineral suggesting felspar. The section is also
spotted with minute scales of green biotite. Augite, some of which
is fresh, is present ; but one phenocryst with inclusions of felspar was
noticed decomposed to a serpentinous product. Considerable quanti-
ties of titanite, some ilmenite, leucoxene, pyrite, apatite, zircon, fluorite
and lepidomelane are also present. The section represents an alkali
rock, and is probabh^ allied to the mica-phonolites.

Other dykes than these above described are also occasionally met
with, but they have not been examined petrographically.

CAMHRO-SILUHIAN.

Marine The transgression of the sea far up the valley of the Ottawa durintr

invasion of ,-r.,.. ,, , ,, .,„

early Paheo- early Palieozoic times, has long been a well ascertained fact, and the

zoic.

charact

Palieoz

with th

conglori

evidenc

the LTti

duratioi

about tl

elevatio

of the I

area to i

It set
Ottawa
extent a:
Silurian,
ex tend in
Ontario f
occupied
of the aei
and smal
forces of
river bet
water co
which we
present a
ing that
valley of
interior b
character
on the M;
outliers of
the west a

To the
likely that
and a shor
cealed ben
and islands
satisfactory
account foi
ments of C(
that are ii

UANLOVt

CAMBR0-8ILURIAN.

119 I

character, thickness and fossil remains of the numerous and extensive
Paheoz. lie outliers have been described. The marine invasion began
with the shallow- water conditions indicated by the deposition of the
conglomerate and sandstones of the Potsdam, and ended — so far as
evidence is afforded by the exposures of strata below Mattawa — with
the Utica. This submergence must have been gradual and of great
duration, the ocean reaching its greatest depth and extent in this area
about the close of the Trenton period, when a comparatively rapid re-
elevation of the land took place, as indicated in part by the deposition
of the Utica shale, and ending with the final emergence of the whole
area to conditions of dry land.

It seems probable that the depression at present occupied by the Extent of
Ottawa River, which in past geological time was of much greater ^^_
extent and importance, formed, during the deposition of the Cambro-
iSilurian, a large gulf or arm of the sea, with transverse bays or inlets
e.vtending far into the interior of the Archiean plateau of Central
Ontario along depressions which even then existed, and which are now
occupied by the more important tributaries of the Ottawa. This arm
of the sea certainly extended as far up the Ottawa as the Mattawa,
and small exposures of arenaceous limestones which have escaped the
forces of denudation occur at intervals in the immediate valley of the
river between Pembroke and Mattawa. The comparatively deep-
water conditions indicated by the deposition of these limestones,
which were certainly of much greater extent and volume than at
present appearing, furnishes strong presumptive evidence for believ-
ing that the sea was continuous in the form of a strait, through the
valley of the Mattawa River, thus connecting directly with the vast
interior basin of Western Ontario in which strata of sinular age and
cliaracter were being deposited. The Cambro-Silurian known to occur
on the Manitou and Iron Islands in Lake Nipissing, are doubtless
outliers of the belts of rocks of the same age which outcrop further to
the west and south-west.

To the north, up the main valley of the Ottawa, it is perhaps it,s northern
likely that the sea extended as far as the head of Lake Temiscaming extension,
and a short distance beyond, and that strata then deposited lie con-
cealed beneath the Niagara limestones that outcrop on the shores
and islands of the nt)rthern part of this lake. This seems the most
satisfactory explanation that can be offered, at the present time, to
account for the presence of numerous often large and angular frag-
ments of Cambro-Silurian strata with embedded characteristic fossils,
that are found lying loose at intervals along the shores of the

120 I

NIPISSINO AND TEMISCAMING REGION.

■ii \

Outliers of
Iron Island.

Outliers of

Manitou

Islands.

northern part of the lake, and which certainly afford no evidence of
having travelled any great distance from their source.

Chazy, Birdseye and Black River Formations.

On the west side of Iron Island in Lake Nipissing, beds of chocolate-
brown and yellowish-gray, coarse sandstone or grit, occasionally becom-
ing a fine conglomerate, rest unconformably on the upturned edges of
the gneissic rocks classified as Laurentian. The rock is composed of
loosely compacted and rounded grains of quartz more or less abun-
dantly coated with hydrous oxide of iron with little or no interstitial
material. The lowest beds are of a brown colour, with occasional
lighter .spots from which the iron oxide has been removed, while
higher beds are yellowish-gray, also showing lighter coloured
areas. When subjected to the action of the weather, curious
subspherical rings suggestive of concretionary action appear on the
exposed surface, but a close inspection shows no appareiit differ-
ence either in composition or texture of the part where these are
developed. The 'neds are of good thickness, but would be useless for
building purposes on account of the loose and friable nature of the
sandstone. Little or no calcareous matter is present, which is a rather
unusual feature, as even the coarse arkose or congiomerative lying at the
base of the Manitou Islands outliers contains a considerable admixture of
carbonate of lime. Murray* mentions the finding of loose fragments
of limestone with characteristic Chazy fossils that possil,)ly overlies
these sandstones, which may thus represent the basal portion of the
Chazy formation.

The Manitou Islands, five in number, are situated about the middle
of the wide open space in the eastern part of the lake. The largest
and most northerly of these islands is about a mile in length from east
to west, and is known as the Great Manitou or Newmans Island-
The next in size and importance is the Little Manitou or McDonalds
Island, while the other three are so small and insignificant that they
have not been separately named.

The most southerly of these islands is somewhat less than a quarter
of a mile long, but only a few chains in width. On the south-east side
of the island is a dark-brown arenaceous limestone, containing angular
or subangular fragments and pebbles of the subjacent gneiss. This rock
i.s t'i c great thickness, and passes rapidly upward into a yellowish-
^; -> . "iitceous limestone. The whole section exposed is of small

! ' an i thickness, the beds lying in nearly, if not quite, horizontal
suc<i*ssic>.i. The shore is strewn with large angular blocks of the

*Report of ProgrosB, Geol. Surv. Can., 1853-56, p. 125.

•]

CAMBKO-SILURIAN.

121 I

coarse-grained, yellowish-gray, arenaceous limestone, containing many
weathered and waterworu fragments of obscure oephalopod-like remains.
These fragments, according to Dr. H. M. Ami, who has examined
them, resemble the Eudoceras multitubtdatum (Hall) from the Trenton
and Black River.

McDonalds Island, or the Little Manitou, is about half a mile in ,, ., .^

' ' On ^icDon-

length from north to south and of no great breadth. At the south- alrls Ishuid.
west corner is a small patch of yellowish -gray limestone, occurring in
beds which have little or no inclination. The only fossil remains
visible at this locality were fragments representing chiefly the
siphuncles of orthoceratites together with crinoid stems and casts of
suppof^ed worm-burrows. Small outlying patches were also noticed
beneath the surface of the water.

About the middle of the island, on the west shore, the thickest expos-
ure of the whole of these outliers is exposed. The total thickness is
about thirty feet, the beds showing a gentle inclination to the west.
At the base is a greenish or yellowish arenaceous limestone holding
decomposed fragments and pebbles of the gneissic rocks beneath. This
is overlain by a yellowish, arenaceous limestone, comparatively free
from coarse fragmental material, which in turn gradually passes up-
ward into gray limestones and shales holding numerous fossil remains.
The orthoceratites are characteristic and numerous, and one specimen
obtained must have belonged to an individual over six feet in length.

The following lists of fossils have been prepared by Dr. H. M. Ami
from collections made by myself and my assistant, Mr. A. M. Camp-
bell :—

Palceophylliim or Columriaria, imperfectly preserved.

Amplexopora, sp.

Coscinopora (1) sp.

Monotrypella qiiadrata, Rominger.

Pachydiclya acuta, Hall.

Plectamhonites (?) sp.

Zygospira recitrvirostra, Hall.

Orthis tricenaria, Conrad.

Rajinesqidna Cf. R. alternata, (Emmons).

Trochonema umhilicatum, Hall.

Small exposures of the basal conglomerate and overlying arenaceous i,\,^j,ils from
limestone occur on the west side of the Great Manitou Island, these <'i«'at
rocks dipping south < 5", while on the south shore, near the old wharf, island,
is a small outcrop of arenaceous limestone dipping east at a low angle.

t ■:■

■ i'

! i

"'-'""■""•"

122

NIPISSING AND TEMISCAMING REGION.

I'.''
Iff

i!i

J i

Trenton
outliers.

Fossils.

From these expo.sures the following fossils were obtained : —
StronMtocerium rugosum, Hall.
Columnaria Ilalli, Nicholson.
Fragments of crinoidal columns not determinable.
Ptilodictyafalciforinis, Nicholson,
Kafinesquina Cf. R. alternately (Emmons).
Zygospira recurvirostra, Hall.
Zyyospira (?) sp. undet.
Lophospira bicincta, Hall.

" sp. type of L. helicteres, Salter.

Maclurea (?) sp. undet.

Actinoceras sp. Cf. Actinoceras Bigshyi, Stokes.
Endoceras, sp.

Orthoceras, sp. Probably a new species of the type of Orthoccras
rapax, Billings. This may be referable to the genus Cameroceras.

Trenton.

Between Deux Rivii'res and Mattawa, are several small comparatively
flat-lying exposures of sandstones and limestones resting upon the
Laurentian gneiss close to the edge of the river, that are com-
pletely covered during times of freshet. The sections exposed are of no
very great thickness or extent, the beds dipping in a southerly direc-
tion at a low angle. The most important of these outliers is the one
situated on the north side of the river about four miles above
Deux Rivieres. The basal or sandstone beds formerly furnished
material for the manufacture of grindstones of an excellent ({uality
while local limekilns utilized certain portions of the higher beds
exposed in this escarpment.

About six miles below Mattawa, two small outliers of a light-
yellowish and purplish, gray-weathering arenaceous limestone are seen
in the north bank of the Ottawa River, containing abundant
fossils characteristic of Lower Trenton period. Besides the rock
in situ, the beach in the vicinity of these outliers contain a large
number of somewhat water-worn blocks of these fossiliferous strata.

Thr following list of fossils has been prepared by L»i. Ami from a
collection made at this locality.

Receptacnlites occidentalis, Salter.

Crinoidal fragments too imperfectly preserved for identification, but
may belong to Glyptocrinns.

Prasopora Selwyni, Nicholson, (J'rasopora lycoperdon, Vanuxem.)

Streptelasma corniculum, Hall.

Frondose monticuliporoid (section required for identification.)

■ARLO)*.

Bra

Obs

cornpat
Stro
Hafi
Orth
Orfh

^ygo

Your
Tjagi

The :

the nor

tional ir

by Logai

separatee

to exist,

of marini

strata of

connecte(

previousl

trough c(

outlier, a

bordering

Although

exposed o

exposed fi

of this out

analogy w

It has

lithologica

Winnipeg

Hudson B

both prese

earning out

in which tl

Bay were

arated fron

*RfIK)rt of ]

pp. 334-33(!.

t Geology of

■ARLOW

]

siluria:?.

123 I

Branching form of monticuliporoid.

Obscure monticuliporoid form, probably related to Solenopora (Cf. S.
conij)acta, Billings.)

Strophomena incurvata, Shepard.

Jtajiesqnina alternata, (Emmons).

Orthis, sp. Cf. 0. tricenaria, Salter.

Orthis (Dinorthis) proavita, W. and Sch.

Zygospira recurvirostra, Hall.

Young of Murchisonia (possibly Lophospira hicarinata, Hall.)

r.'agment of trilobite too imperfectly preserved for identification.

Silurian.
Clinton and Niagara.
The rocks of this a"e, exposed on the shores and islands of Clmracter and

. . t e athuities of

the northern portion of Lake Temiscaraing, have been of excep- tlu- Silurian
tional interest to geologists ever since their discovery and description '"" "^'^ *'
by Logan in 1845*. (Jeographically, this outlying patch is so widely
separated from any locality where rocks of similar age are now known
to exist, that it has been a question whether it is indicative of an area
of marine submergence connected with that in which the fossiliferous
strata of Hudson Bay were deposited, or whether it was in some way
connected with the Niagara basin to the south-west. It has been
previously asserted that these rocks belong rather to the great northern
trough connected with Hudson Bay, of which they are probably an
outlier, and the absence of all strata of Niagara age in the region
bordering the lower Ottawa has served to strengthen this belief.
Although in lithological character and colour the rocks of similar age
exposed on Temiscaming exhibit a marked similarity to the Niagara
exposed further to the north, the rich and varied fauna characteristic
of this outlier presents no corresponding resemblance, but rather a close
analogy with the Niagara formation of south-western Ontario.

It has been shown that a pronounced similarity exists both in Fauna tuilike
lithological character and fossil remains between the Niagara of the ,^.n'J'^siluri-in
Winnipeg basin and that exposed in the vicinity of the Churchill on
Hudson Bay, although these areas are now widely separated, while
both present organic forms that are entirely lacking in the Temis-
caming outlier. These facts, therefore, seem to prove that the seas
in which the Niagara sediments of the Winnipeg basin and of Hudson
Bay were deposited were practically continuous, while both were sep-
arated from the Teraiscjiming basin and the region to the south west.

*RejK)rt of ProgreBs, Geol. Surv. Can. 1845-40, pp. ti9-70.
pp. 334-33(i.

t Geology of Canada (18(13), p. 334.

Geology of Canatla (1803),

124 I

NIPIS8INQ AND TEMI8CAMINO REGION.

ill

I 'J

.strata in
HyiiLliniil
iuriii.

Possible area
of Cainbro-
Siliu'iaii.

Conditions of
deiwsition.

The stiiita forming the Temiscaming outlier occur in the form of a
shallow synclinal trough, occupying somewhat more thnn the breadth
of the lake, which is here about six miles, and extending from
the northern end of Moose or Bryson Island, north-westward
beyond the confines of the present map. On both sides of the
lake the rocks incline towards th« water at varying angles, de-
pending on the character of the shore-line ; although in general
the dip does not exceed 10', and angles of lesser amount are far
more common. On Mann or Burnt Island, as well as on the
peninsula to the north, the limestones show a very gentle westerly
inclination of between one aiid two degrees, while on Percy Island,*
near the west shore, the rocks are very nearly if not quite horizontal.
It is thus evident that any section made must of necessity be
more or less ideal and any thickness based on the observed angles of
the dip is sure to be misleading. The whole thickness exposed in any
one section is somewhat less than 150 feet, and it seems certain that
the total amount of the Niagara exposed on this lake cannot be groa''^?r
than 300 feet, and may be considerably less. The occurrence of loose
angular fragments and slabs of grayish dolomite, resembling that
exposed in the vicinity of Lake Huron and Nipissing and containing
characteristic Trenton fossils, has been noticed.! These are distributed
at several points on the shores of the lake and specimens were collected
from the north-east shore of Chiefs Island. Although their source has
not yet been ascertained, the angular character of the fragments and
their abundance shows clearly that this cannot' be far distant. The
lake is here over 200 feet in depth and it is just possible that below
the Niagara limestone and concealed beneath the waters of the lake
there exists an area of Carabro-Silurian rocks. This, however, can
oniy be ascertained by boring, as no exposures of these rocks were
encountered, although a diligent search was made with this object
in view.

The relatively smaller quantity of conglomerates and sandstones,
characteristic shallow water deposits, and the rapid alternation from
these coarser elastics to the fine-grained limestones indicative of deep
water deposition, point to a rather sudden marine invasion ; while the
comparatively great volume of strata remaining shows a prolonged
submergence. The fine-grained character of most of the limestones
show that their deposition took place in a quiet arm or extension of
the sea, not affected by the open ocean, while the abundance and char-

* So called in honour of Captain Walter Percy of the steamer Meteor plying on
this lake,
t (.Jeology of Canada (18()3), p. 335.

BARLOW.

acter c
of its

of the

coherei

gioiner,

have a

consist]

adinixt

the und

yards in

relation;

pact an(

occurs in

arenaceo

at an an

At Ha

edge and

yellow fii

north-eas

of the coi

Niagara e

perhaps tl

underlying

be benoatl

Further

and is sep

narrow chi

senting a

weathering

from yellov

Shells of V

number of

Ami, as foil

Clathrodi
Favosites
Syringopi
Crinoidal
Leptcena r
Atrypa rei
Meristella
Anoplothet

]

SILURIAN.

125 I

acter of the fossil reinaias are ample testimony of the genial character
of its waters.

As exposed on the west side of Wabis Bay, in tlie north-west corner ('"ubIkuiii--
of the lake, the lower portion of this formation is composed of a loosely «toneH.
coherent sandstone or grit alternating with thinner beds of a fine con-
glomerate, with pebbles chiedy of Huronian quartzite, most of which
have a thin coating of yellowish or brownish iron oxide, while the matrix
consisting of similar material in a finer state of division, contains a slight
admixtuie of calcareous matter. The actual contact between this and
the underlying slate of the Huronian is not seen, although only a few
yards intervene between the exposures of the two rocks. The existing
relations can, however, be made out pretty clearly, for while the com-
pact and rather massive slaty rock which here represents the Huronian
occurs in exposures with more or less rounded or hummocky outlines, the
arenaceous strata of the Niagara dip off or away from these hillocks
at an angle of 5°.

At Haileybury, on the western shore of the lake, close to the water's Limijstone
edge and cropping out from the shingle is a small exposure of light- i',',,,"..
yellow tine-grained limestone, without visible fossil remains, dipping
north-east 25^ The discovery of limestone with the general contour
of the country in its vicinity, seem to suggest that a small patch of
Niagara extends northerly along this shore towards Wabis Bay, being
perhaps three miles in length by about a (juarter of a mile in breadth,
underlying the clay which here eflfectually conceals any rocks which may
be beneath.

Further south, on Percy Island, which is only a few chains in length Foshils from
and is separated from the western mainland by a very shallow and
narrow channel, the rock exposed is a light-yellowish limestone, pre-
senting a very uneven or cavernous surface as a result of unequal
weathering. The strata are nearly if not quite horizontal and weather
from yellow to brown or almost black, as a result of the iron present.
Shells of various species of brachiopods are somewhat numerous. A
number of the fossil remains collected, have been determined by Dr.
Ami, as follows : —

Clathrodictyon fastigiatum, Nicholson.

Favosites Gothlandica, Lamarck.

Syringopora verticillata, Goldfuss.

Crinoidal fragments.

LepUena rhomboidalis, Wilckens.

Atrypa reticularis, Linnseus.

Meristella, sp.

Anoplotheca hemiapherica, Sowerby.

in ffl: •

! ll

. Jl

; ; 1

126 I

NIPI88INO AND TKMISCA.M1NO REGION.

MRLOW.

Cdinjldiiiilatf
on ( /'liit'fs
I Inland.

la '

Pterinea, sp.

Also branches of obscure Monticuliporidu'.

Thia fauna represents the Clinton or base of the Niaj»ttra or lower
part of the Silurian.

The northern and western points of Chiefs Island, rise into compara-
tively high ridge.s of massive (juartzose sandstone or (juartzite-grit
which present the usual rounded and glaciated outlines. Sheltered in
the bay intervening between these two points is a small patch of boul-
der conglomerate, composed of sub-angular masses derived from the
underlying quartzite. These aie imbedded in a calcareoarenacoous
matrix composed chicHy of pebbles and finer material, the whole repre-
senting evidently a boulder-strewn beach covered by later sediments of
the Niagara formation. The surface of the quartzite on which this con-
glomerate rests, presents the humniocky character so common in the case
of the hard Archa-an .strata, the irregular cracks and depressions being
filled by the conglomerate. Subsequent glaciation has removed much
of the material, .so that the exposure now presents a plane surface with
a more or less net-like structure, the framework being represented by
the finer arenaceous cement while the meshes or interstices are occupied
by truncated sections of quartzite boulders as well as of the rounded
hillocks of the solid rock beneath. Some of the boulders present in
this conglomerate were evidently large concretions, as they exhibit
concentric structure and weather very rusty owing to the disintegra-
tion of the large proportion of iron present. The finer cementing
material, whil(> relatively much smaller in amount than the peebles and
boulders, is always of a greenish or yellowish colour and frequently
contains corals and orthoceratites. The action of the weather has par-
tially obliterated the glacial strife on this finer matrix, but the sections
of the quartzite boulders and hummocks exhibit these markings in great
perfection.

.^ ., , On the south-western shore of Chiefs Island, is another small patch

r ossils from ' _ '^

Cliiifs Island, of a finer grained conglomerate, the pebbles of quartzit^^ being less
numerous and of much smaller size, while the matrix conrai is much
more calcareous matter. The rock dips south-east < o\

A number of rather badly preserved fossils were secured at this
locality, which have been named as follows by Dr. Ami : —

Halysites catenularia, Linnieus.

Columnaria, sp., with very irregularly disposed horizontal tabula\

ZaphrentiSf sp.

Streptelasma or Caninia, sp.

Rhynchonella, sp.

Murchisonia, two species.

Euomp
Discoso

The ab(
of the Ni

On the
within le.s!
occupied I
of the Nil!
already de
gular fragi
of the expi
cement of
corals and

This bot
in turn re
rather frial
closely foil
with a gen<
action of t
unevenly le
distance no
deposits.

In the
Wright's si
light-yellow
erly directi
small patch

On the
there are tw
at the shore
dipping in
these small

On Burnt
between thi
well as on t
the northerr
that represe
is of a pale-
in thickness

Mmowc

SILURIAN.

127 I

Outliers on
cM-^t -idc of
lakt'.

]'>asal con-
^'liiiiienkte.

Eiiomphalus, very large species.
Dlscosoru8. Cf. D, conoideus, Hall.

The above fauna represents the Clinton formation or lower portion
of the Niagara.

On the east side of the lake, from the point south of Chiefs Island to
within less than a (juarter of a mile from Piolie Point, the shore is
occupied hy a narrow fringe of the basal conglomerates and sandstones
of the Niagara. The coarser beds are of the Ijoulder conglomerates
aheady described, representing simply a talus of angular and sub-an-
gular fragments detached from the elevations in the immediate vicinity
of the exposures, consolidated together by a finer grained arenaceous
cement of a yellowish colour in which are also embedded fragments of
corals and orthoceratites.

This boulder conglomerate passes upward into a tine conglomerate
in turn replaced by a coarse grit, and becoming finally a yellowish
rather friable sandstone. These beds run in long ui^dulating curves,
closely following the general outline of the underlying quartzite
with a general westerly dip at angles varying from 10' to 15\ The
action of the waves has in places caused this to disintegrate very
unevenly leaving a rough pitted surface. At Piche Point and for some
distance north, the Huronian quartzite is left entirely denuded of these
deposits.

In the bay to the south of Piche Point and between this and Aienact'ouN
Wright's silver mine, there are two small patches of thinly bedded ""^'' ""''
light-yellow arenaceous limestone dipping in a southerly or south-west-
erly direction < 5°, immediately south of Wright's mine is another
small patch of similar arenaceous limestone dipping south-west < 9°.

On the east shore of the lake, nearly opposite Bryson Island,
there are two more small patches of the arenaceous limestone exposed
at the shore, wrapping round the hummocks of Huronian quartzite and
dipping in a southerly or south-westerly direction <5°. None of
these small patches of limestone contained any visible fossil remains.

On Burnt or Mann Island, as also on the two smaller islands >iaiii Imu'-
between this and Bryson Island (Oster and Brisseau islands), as ^^'^^^' '^^^'^'
well as on the high promontory separating Wabis and Sutton bays in
the northern part of the lake, are exposed the limestones and shales
that represent the deep-water deposits of this period. The limestone
is of a pale-yellow or cream colour, weathering whitish, and varies
in thickness from a few inches up to two feet or over. Some of the

r , .^

Biiildinp

wtunt'.

■I

Fossils from
Mann Island,

illf

128 I

VIPISSINO AND TEMISCAMIXG REGION.

beds are very fine-grained and of rather even texture, and it is
possible that some parts may prove to be sufficiently uniform for use
as lithographic stone. Asa building stone it is of excellent quality.
These lime, tones, on the north shore of the lake at Dawson Point, dip
a little south of west at an angle of between one and two degrees,
rising into cliffs of over a hundred feet in height on the west side of
Sutton Bay, and forming a somewliat elevated rocky plateau with a
gentle westerly slope, corresponding mainly with the angle of dip
t<owards Wabis Bay. The east shore of Mann Island presents a some-
what similar, though much lower escarpment, while the western shore
is a gently shelving beach, which at low water reveals consider-
able areas of the almost horizontal limestones. Some of the beds con-
tain a considerable proportion of silica of a cherty character, and all
the fossils are more or less silicified. The action of the weather
causes them to stand out in relief and often displays their minute
structures perfectly. A large collection of these fossils was made
along the western shore of Mann Island, comprising the following
forms as determined by Dr. Ami and Mr. L. M. Lambe : —

Bythotrephis (Chondrites) gracilis, Hall

" Cf. B. palmala, Hall.

CJathrodictyonfastigiatum, Nicholson.
Cyathophyllum articulatum, Wahlenberg.
Zaphrentis Stokesi, Milne-Edwards and Haime.
Favosites Gothlandica, Lamarck.
Alveolites JViagarensis, Romiiiger (non Nicholson).
Cladopora crassa, Rominger.
Syringopora verticillata, Goldfuss.
" bifurcata, Lonsdale.

Ualysifes catenularia, Linnaeus.
" compacta, Rominger.
Lyellia ajinis, Billings.

" Americana, Milne-Edwards and Haime.
Thysanocrinus liliiformis. Hall.
Dendrocrinus longidactylns, Hall.
Taxocrinus n. sp.
Lichenalia concentrica. Hall.
Pha-nopora expansa, Hall.
Trematopora sp.

Ortliia (Dalmanella) elegantula, Dalman.
Orthis calligramma, Dalman.
Platystrophia biforata, var. lynx, Eichwald.
Strophomenoid shell, type of Rafinesquina.

BARLOtV. I
St.

Le
At

Tr
Pe
Eu
Mu

Dis

OrL

Ort)

Acti

Call

Blumenb

Beyr

The PI,
the main
snow and
This is bt
regional u
this came
invaded i
gulf, riva
sea during
seem to s
ocean cove
Hudson B
over a ' as
the Great

Taylor,
been at
correlatinjr
ence, but ii
point out
obtained.
9

-J

PLEISTOCENE.

129 I

Stropheodonta sp. (? n. sp.)
Leptana rhomboidalis, Wahlenberg.
Atrypa retictilaris, Linnreus.

" intermedia, Hall.
Trematospira sp.
Pentamerua ohiongus, Sowerby.
Euomphalus alatus, Hisinger.
Murchisonia sp.

" subulata, Hall.

Discosorus conoideus Hall.

" gracilis ? Foord.

Orthoceras, sp.

" sp. Cr. 0. virgidatum, Hall.

Orthoceras Cf. 0. Cadmus, Billings. C£. 0. sub-cancellatum, Hall.
Actinoceras! vertebratum, Hall. . A. Backi, Stokes.
Calymene Niagarensis, Hall. Probably identical with Calymene
Blumenbachii, Brongniart.

Beyrichia, sp. Cf. B. lata, Hall.

PLEISTOCENE.

The Pleistocene history of this and adiacent regions seems to be in IMain division
the main divisible into two parts. (1) That of great accumulation of
snow and the production and maintenance of a confluent ice-sheet.
This is believed to have been accompanied, if not caused, by a vast
regional uplift, increasing in amount to the north-eastward. Following
this came (2) a profound submergence, during which time the ocean
invaded a large portion of the Ottawa valley, forming a marine
gulf, rivalling in extent and depth similar encroachments made by the
sea during portions of the Paliwozoic. The researches already made
seem to show that channels may have conrcoted tlua portion of the
ocean covering the St. Lawrence and Ottawa valleys with that existent in
Hudson Bay, while the marine invasion may even have been continuous
over a ast inland basin represented at present in part by the area of
the Great Lakes.

Taylor, Chalmers, Gilbert, Wright, Spencer and others have Subsidemps
been at work in this and neighbouring districts connecting and t"rrac«^r '^
correlating the beaches representing the various stages of this submerg-
ence, but it is only possible within the scope of the present report to
point out in the most general way some of the important results
obtained. Taylor has shown that immediately following the retire-
9

•■n r ;

Iii||)

i ^li

iii'^

ii.

11 i'

^li

• .

J I

- '

130 I

The confluent
glacier.

Glacial and
intt<rglaci;il
imriods.

NIPISSING AND TEMISCAMIN'G REGION.

rnent of the great ice-sheet which marked the first part of the Pleisto-
cene, and to which reference will shortly be made, an important strait
or arm of the sea covered the Mattawa and Temiscaming valleys, while
later, as the flood subsided and the ice receded from parts of the area
previously held by it, most of the waters of the Great Lakes emptied
for a considerable time eastward into the Ottawa through the Mattawa
valley. Beaches marking the successive stages in the subsidence are
well exposed on the hillsides to the north and south of Lake Nipissing.
especially in the vicinity of North Bay, where they were found and
described by Taylor and Wright, vhile the valleys of both the Mat-
tawa and Ottawa rivers present many evidences of having been occu-
pied for a somewhat protracted interval by a stream rivalling, if not
exceeding, the St. Lawrence in volume.

In the present report, the existence is assumed of a vast superincum-
bent glacier, of which the chief gathering-ground, as indicated by exist-
ing striif and distribution of drift material, was situated directly over
the watershed between Hudson Bay and tlie St. Lawrence River. This
hypothesis appears to offer the most satisfactory and comprehensive
explanation of the various phenomena, while at the same time it is one
in accord with views that have already received most general recognition
among students of Pleistocene geology.

Although thus generally agreed as to the agency producing the vari-
ous results encountered, a considerable diversity of opinion exists
among geologists as to whether the large number of observations
already made ean be adequately explained on the theory of one great
ice-flow with minor oscillations or of several distinct epochs of glaciatiou,
each with its own proper ice-mass and separated from one another by
interglacial periods during which much milder climatic conditions pre-
vailed. The information obtained from the examination of this district
is not suflicirnt to afford a basis of -irgument in favour of either view.
It is, however, easy to understand that while areas situated near the
extreme border of the ice-sheet may have enjoyed comparatively long
interglacial periods, during which the climate was of such genial
character as to permit and favour the growth of a somewhat luxuriant
vegetation, others, in regions further removed to the north-east and near
the centre or centres of accumulation showed very little, if any,
amelioration of temperature. The divergence in existing stria> observed
throughout this district seems perfectly explicable on the theory of
differing phases of one great glacier, with comparatively short interven-
ing lapses of time during its temporary recession and subsequent
re-advance.

■]

PLEISTOCENE.

131 I

As the position of these first-formed ice-masses would of recessity be Where glac-
11.1, . n,,. • "'•''* were nrst

largely determined by the position of the highest land then existent f.unud.

in this region, it is probable that very early in the Glacial period there

were two main gathering grounds or centre.s of dispersion for such ice.

These would be situated respectively in the area to the north-west of

Lake Teniiscaming, in the vicinity of the " Great Bend " of the

IMontreal River and the high quartzite ridges to the west of Lady

Evelyn Lake, and on the high rocky hills known to exist in the

vicinity of the height-of-land to the north-west of Lake Temiscaming.

It is probable that early in the ice age these local centres sent out T'"|ct's of

_ "' ° I'iirly glaciers .

glaciers which flowed over the lower lands and valleys to the south

and may have been the cause of some of the striie observed on the
rock-surfaces exposed in the valley of the Montreal River, as well as on
the shores of Lake Temiscaming. Although it is possible that all
such evidences may have been so obscured in the profound general
glaoiaticii which followed as to render their recognition and correlation,
mdters 'v" (»x,reme difficulty. We may suppose that local glaciers of
tliii \dnO above referred to, increasing under favourable conlitions,
eventually coalesced as parts of one great ice-sheet, of which the
distributing centre may have been gradually shifted eastward towards
the neighbourhood of Opasatika and Labyrinth lakes on the canoe-
route to Lake Abitibi. There is likewise sufficient evidence, afforded
by a study of the later striations, that must have been caused by
temporary re-advances in the waning ice-sheet, that this eastward
shifting of the main gathering-ground must have slowly continued,
while the final recession was almost directly north-east.

Tt is now a well ascertained fact that the motion of ice is one result- Conditions
« . , . . , ,. , . 11 1 11 iit'terniining

ing from its phi: ' city, resembling substantially the movement which (Hnction of

obtains in an extrHi-iely tiiick and viscid fluid when spread upon any "'"''•""
surface and a H!.;i}>ly ft' froah material constantly added. It is there-
fore obvious t' at *»\j. mclination, however slight, of the underlying
surface or the interp>>. '♦:ion of natural barriers at or near the sources
of supply were ii the u Vit instances the deteniiining causes of the
general direction of the ice flow. This onward motion once imparted,
was continued and depended subsequently not so much on the nature
of the land surface on which the glacier reposed as upon the general
slope of the upper surface of the glacier which inclination was imparted
as a result of the unequal accumulation of material at the centres of
dispersion. Y- the north nnd north-east of Lake Temiscaming the
various passe:.. ' . valleys leading northwards across the height-of-land
are a little lesstji-:. iOOO Ceet above the sea, although thb ^ncky ele-

132 I

NIPISSING AND TEMISCAMING REGION.

illli

Differential
uplifts.

Transjxjri-
ation of
material.

Distance of
transix)rt.

Direction of
transix>rt.

Stratified
deposits.

rations in the immediate neighbourhood rise in general from 200 to
500 feet heigher, while some of the hills in the vicinity of Labyrinth
and Opasatika lakes show an ele.ation of over 600 feet above the
surrounding lakes. If added to the general slope thus obtained be
taken, the rise consequent on a diflferential uplift gradually increasing
in a northerly direction, the resulting slope would be sufficient to
compel a somewhat rapid south-westerly flow in any glacier formed in
this vicinity, while in addition it is probable that an ever increasing
supply of icy material to the north-east, might so accelerate this onward
motion that even the interposition of such formidable natural barriers
as the deep gorge of Temiscaming must have been, with its steep
opposing slope, only served as temporary checks.

This great ice-sheet acted as an important agent of transportation,
catching up and carrying forward 1; :.;;" quat titles of clay, sand, gravel
and boulders from the higher elev. ; "^ the north to fill up the

various inequalities of contour existiu. ither south. The drift
material, though varying very much in thid region, is as a rule very
coarse on the higher levels and on the hill-sides facing towards the
south and south-west. On these higher levels the ground is very
much encumbered by more or less rounded or subangular boulders
which usually do not show transportation from any great distances ;
although by a careful comparison of the material of this drift, it was
ascertained that many of these loose fragments had been carried as
much as fifty or sixty miles, in a direction closely corresponding with
the striation marking the maximum extension of the ice-sheet over
this district. Thus, loose fragments of the buflF-coloured limestone
with characteristic nodular cherty matter, known to occur in a patch
of somewhat limited area in the vicinity of the northern part of Lake
Temiscaming, were found on Marten or Crooked Lake in the town-
ship of Gladman, a distance of over fifty miles from where such rock
is now found in place. The distribution of these characteristic frag-
ments which are an especially valuable criterion of the direction of ice-
flow, on account of the known limited extent of this Silurian outlier,
shows that the agency which aflfected their transportation had a
direction of movement varying from S. 7° W. to S. 18° W., thus
agreeing very closely with the most abundant and pronounced striae.
On Lake Nipissing, the various shales and grey wackes characteristic of
the Huronian exposed in the area of the Lake Temiscaming map-sheet,
are rather pl'-atifully represented among the loose boulders fringing
the shores.

The stratified sands and clays SvO abundant in the area to the north
of Lake Nipissing, as well as those in the vicinity of the Veuve River,

•J

PLEISTOCENE.

133 I

were probably deposited very rapidly from streams issuing from the
margin or front of the retreating glacier, as was likewise no doubt
the case with the thick and widespread deposits of stratified clay
which forms such extensive flats in the region bordering the northern
portion of Lake Temiscaming. The terraces characteristic of the occur-
rence of these clay deposits to the north of Lake Temiscaming, merely
serve as mark accentuating the various stages or baitings in the ice-
sheet, of which the margin was buried beneath the rising waters, thus
permitting and even favouring such a mode of deposition of the englacial
detritus. Especially along the course of the Ottawa and Temiscaming Moraines.
valley, the region exhibits frequent great accumulations of morainic
dflbris marking the recession of the ice-lobe occupying this deep and
important depression. These deposits from the drift-laden glac'&rs
are described in some detail in the geological description covering the
area immediately bordering these topographical features.

Besides the removal and transportation of boulders, gravel and ( Jlaciation of
other material, there is abundant evidence everywhere of considerable '"''" '''"'^ ^^'
abrasion of the surface produced by the passage of the ice-sheet across
this district. Throughout the whole area covered by the accompanying
map-sheets, most of the rocky elevations have been smoothed and in
many cases even polished, while scratched or striated surfaces are also
common. These striie are usually long, more or less parallel scratches,
varying in size from extremely tine lines which can often only be
detected by very close scrutiny, to furrows several inches in depth and
width. They have in general a somewhat constant direction except in
the vicinity of deep and narrow valleys, where they frequently show con-
siderable divergence from the average direction of the district. Many
of these striu» consist of a series of irregular, curving and often faint
scratches, as if occasioned by an uncertain or intermittent action while
some of the deeper and more pronounced furrows exhibit irregular
broken cavities at intervals in their course as though produced by <i
" bumping " action caused by hitches in the rocky implement produc-
ing them.

Ledges and ridges which have been long exposed to the action of the differences in
weather, usually reveal little or no evidence of such striation on account I '"^ '
of the sub-aerial decay to which the rock has been subjected, while, on
the contrary, rock exposures which have been but lately denuded of
their overlying soil, as well as those portions of the rocky shores of the
various lakes and streams exposed only between extremes of high and
low water, usually exhibit such markings in great perfection. The
various gneisses and granites of the Laurentian areas are so faintly

spp

^lili

134 I

IflPIBBING AND TEMISCAMING REGION.

BARLOW.

marked, if at all, that the direction of the strise can seldom be ascer-
tained with any degree of certainty. There seems no reasonable doubt
that such markings were originally present, as under the favourable
conditions already mentioned they are often plainly discernible, but as
a rule prolonged atmospheric dec-y has so acted on exposed surfaces of
these rocks that their surfaces have become roughened. On the other
hand on exposures of Huronian rocks such as slate, greywacke, quartzite
and especially diabase and gabbro, these glacial markings are very
Strife in frequently to be observed in all their pristine freshness. In many locali-

different bear- ties, particularly in the area covered by the Lake Temiscaming sheet,
there are two, three and even four sets of stria; on the same rock-surface,
diflfering somewhat in direction and marking as a rule but slight changes
in the direction of the ice-flow, during successive re-advances of the ice-
sheet. The correlation of such stritB is usually exceedingly difficult and
unsatisfactory, ns the intervening lapse of time denoted by these
divergences was doubtless of comparatively short duration.

Probably due
to different
periods.

Change from
south tosoutli'
west.

Striae follow-
ing valleys.

Tt is probable, as has been sfat .>d, that early in the ice age glaciers
of the alpine type occupied the high hills of diabase and gabbro in the
vicinity of the height-of-lanJ 'r .Tiediately west of the canoe-route
between Lac des Quinze and Abitibi, ps well as on the high ridges of
quartzite-grit to the west of Lady Evelyn Lake, of which Maple
Mountain is the most prominent eminence. The striae which have the
closest correspondence with the general trend of the valley of Lake
Temiscaming and the Ottawa River were possibly caused by such a
local glacier, as these markings are earlier than those which trend to
the east on the one hand or to the west on the other. The striaj
marking the main advance of the- ice-sheet in this region show a
general trend of about S. 14° W., but many of the observations noted
present a marked divergence from this general direction, especially
those made in the vicinity of lakes and streams where these ice mark-
ings show an unfailing tendency to conform very closely to the direction
of the inclosing valleys.

The earliest of these south-westerly ice markings are those which
run nearly south, the direction of ice-flow showing a gradual change in
the direction of successive re-advances, following temporary recessions,
from a little west of south to almost directly south-west.

In the area covered by the northern and central portions of the Lake
Temiscaming sheet, there are many lakes whose general trend
makes but a small angle with the average direction of ice-flow
while their containing valleys are narrow, rocky and steep. The
northern part of Temagami, Waibikaiginaising and Wakemika lakes

BARLOW.

]

LIST OF GLACIAL STRIiE.

135 I

may be cited as examples where the glacial strife show a general direc-
tion of a little east of south, in this respect showing the marked influence
of topographical outline.

In the subjoined list, which is necessarily brief and incomplete, con- List of striae,
aisting of observations made during an exploration whose primary object
was to map out and report upon the various subdivisions of the Archwan
rocks, an attempt has been made wherever possible to tabulate in
regard to their age the various striic observed. "Where two, three, and
even four sets are noted as occurring on the same rock-surface, the
order in which they appear is believed to represent, with approximate
accuracy, their relative ages from the oldest to the most recent.

List of Glacial Strict.

Lake Temiscaming.

Wabis Bay, west shore of, on lot 10, con. V. Bucke Township ... - iiAk^-m

Wfibis Bay, east shore of, on lot 2, con. I. Harris Township S 19° E

Sutton Bay, north-east shore of, on lot 8, con. V. Harris Tp .S 51" E

East shore, west of Abbika Creek, on lot .38, con. I. (iiiigues Tp. . S HI" E

Chiefs Island, east shore of a ,.,.o -t^.

Chief.s Island, north shore of S (ifi^ E

rs 14° E

Chiefs Island, west shore of -^ S 48° E

U 54° E

East shore, on lot 31, con. I. Guigues Township S 32° E

( S 33° V

Piche Point, south of, on lot 12, con. I. Guigu(!8 Township ' S 4(j° F

East shore, north of Wright's mine, on lot 7, con. II. Guigues Tp. - L T.jo v

Wright's mine, (Lake Temiscaming Silver Mine) on lot 62, con. I. .
Duhamel Township "Block A"

^ f S *^H° E

Joanne Bay, east shore of, on lot 58, con. I. Duhamel Township.. • 'tjf^^^y

( S *'fl° E
East shore, on lot 54, con. I. Duhamel Township g " j.jj

East shore, at Narrows with Bryson Island on lot 44, con. I. Duha-
mel Township S 21'' E

East i-hore, opposite Drunken Island, on lot 31, con. I. Duhamel

Township S 4° W

West shore on lot 14, con. IV. Lorrain Township S 4° W

West shore on lot 12, con. VI. Lorrain Township S 21° E

( S r'°W

West shore on lot 11, con. VII. Lorrain Township • • I S 18°W

r S 1 8° E
West shore, on lot 15, con. 1. Bucke Township -I y 2(i°'VV

Laperri^re Bay, north shore of, ^ a mile east of old H. B. Co's ( S 21° E

post, on lot 7, con. II. Duhamel Township I, S (1° W

r S IT^W
Islet near east shore about 1 mile south-east of Roche McLean ^ ^ 32°W

Boche McLean, near west shore S 10° E

V/'est shore opiwsite Roche McLean S 4° E

West shore li miles north of Montreal River S 4° W

f S 21° F
West shore 1^ miles south of Montreal River | g j^yoyy

■' ;i (

: I 11:, 1

■■: \\

i 1

I :^

List of
striae— Cont.

136 I

NIPIS9INO AND TEMISCAMINO REGION.

Quinzft River.

Islet opposite North Teiniscaiiiing, P.O. Near south-east shove

I S 21' E
I S 31° K

At second rapid abovu Lake Teiniscaiiiing H 50" E

On new roaci to Lac des Quinze, (5 miles east of First Rapid on

River des Qiunze S 47' E

Lake Temagami.
North East Arm, west end of portage to Caribou Lake ,

rs 4 W

JS14 W

ts l'J"W

North East Arm, Island in south narrows, two miles west of jiortage

to Caritou Lake S WW

North East Arm, Islet near south shore, h mile south-east ofjSlfi'W

Ferguson Island " IS 20 W

Nortli East Arm, island east of IJroom Island S 14'\V

North East Arm, iM)int on south shore A mile south-east of Broom | S 9'W

Island . . . . : t S 24 W

Ko-ko ko Bay, East shore of, Ih miles south of north end H O^W

Kuko-ko Bay, Islet near centre, 2^ miles soutli of north end S 14 \V

Ko-ko-ko Bay, Islet near west side, S^ miles south of north end. ... S S°\V

Ko-koko Bay, East shore of, 3A miles south of north end S G"W

Ferguson Bay, east side, near southern end S 1'^ E

f S (r F
Ferguson Bay, point on west shore 1^ miles south of Ferguson Point ^^ «" w

I S 1° F
Sandy Inlet, point on south-east shore h mile east of Ferguson Point | a -.^o y

' ' E
E
Whitetish Bay, east shore, Ih miles south of creek from Whitefish / S 11"" E

Lake : \S 4\V

Whitefish Bay, p.-uit on west shore ^ mile south-west of creek from

Whitefish Lake S 28° E

Whitetish I5ay, islet in, nearly 1 mile south of creek from Whitefish / S 1° E

Lake i S 1(5° E

i S ^^ F
North Arm, Point on west shore, ^ mile south of Deer Island i S 14° F

South West Arm, island near north end of S 1!)^ W

South West Arm, east shore of, 2 miles south-west of Narrows f S !>^W

Island "I S 19° W

I S 4°W
South-west Arm, east shore of, 5 miles north-west of south end • • • • " ci i- \y

is 1 °
Sandy Inlet, north-east shore, near mouth of Annima-nipissing River | ti i qo

Islet, IJ miles south-west of

fS 4 VV

■^sir

Hudson's Bay Cos iwst -^ S 11°W

tS29'W
Islet Ij miles east of Hudson's Bay Co.'s post S 9° W

Islet near north end of Island Bay

Portage near south end of McLean Peninsula S 4° W

f S 24° W
High Rock Island, south-east shore of i S 2<»° W

Cross Lake.

West shore of lake, IJ miles south of Temagami River inlet S 5° W

North ixiint of island, Ij miles south of Temagami River inlet S 3° W

f S 2° F
East shore of same island, 2 miles south of Temagami River inlet. . -I S 7'> w

West shore, J mile north of Temagami River inlet S 13° W

{S 2° F
S 8° W

Small island near west shore IJ miles north of Te»iagami River inlet. I a i k» w

Point on west shore Ij miles north of Temagami River inlet S 5° W

MRLOW.

LIST OF GLACIAL STRI^.

137 I

Area South-east of Lake Temagami.

Island near south-east end of .Tniuping CarilK)u Lakt' S 14' W

Marten Jiuke, acmth-west shore of, i mile nurtli-we.st of north town

line of McLaren S 20' W

Islet in Red Cedar Lake, lot (i, con. VI., Thistle Township i S l'"" W

Tomiko Lake, north-west shore of, on lot .5, con. I., Fell Township S 1.5^ W

rS 4'W

Moxam Lake, north-east shore of ■! .S 22' NV

ts 2!)' W

Exiiectation Lake S 22° W

Simpson Lake, at outlet ot S 22" W

Sinijjson Lake, islet near north-east end of S 22" W

Mackenzie Tjake, islet near east end of S 22° W

Mackenzie Lake, east end of S 14' W

Breadalbane Lake S 21 ' W

Bush Lake (near headwaters of Ottertail Creek) S 30" VV

Poplar Lake, west .shore of, on lot 2, con. III., Gladman Township S G' W

Kaotisinewaning Lake, south shore of, in Xotnian Townshiii S 7° W

Red Water Lake, west side of, nearly ^J mile from outlet S 20' W

Lake Nipissing.

Goose Islands i u oj.j \y

Manitou Islands, must easterly islet of South

Small island in Goulais Bay S 1.5" W

Goulais Point S 25" \V

Small island opiX)site lot 3, con. C, Caldwell Township S 19" W

North shore of, on lot 7, con. C, Caldwell Township S 25" W

North shore of, on lot 11, con. C, Caldwell Township S 25' W

Point on west shore S 30" W

South-east shore of Bear Bay, opposite Maskinonge island S 10' \V

Deer Bay, south shore of (west arm) S 20" W

North shore of, on lot 6, con. C, Springer Township S 14" W

North shore of, on lot 5, c(m. C, Springer Township S 12' \V

North shore of, point 3^ miles east of Dukis P jint S li)' W

North shore of, point 4 miles east of Dukis Point S 14" W

Clark (Sandy) Island, near western end ' p^' S" ' W

Hardwood Islands, west end of S 20" W

Island east of east end of Hardwood Islands S 25' W

Scuth Bay, east shore of S 23= \V

List of
striuj — Cant.

Lady Evelyn Lake and vicinity.

Point on north side of largest island in Lady Evelyn Lake, 3 miles

south-west of Obisaga Narrows S 4' W

Island in Lady Evelyn Lake, 3A miles south of Obisaga Narrows. . S (5" W

f S 5" \V
South-west shore Nonwakaming Lake, 3 miles west of inlet ' S 21" \V

Island near east shore Nonwakaming Lake, about 2 miles north- / S 3' W

west of inlet 1 S 20" W

I S H" V
West shore Wakemika Lake I S 22' E

r s ^^ 1*^

South shore Wakemika Lake ' S 1"" E

Turner Lake, south-east shore of S 10" W

Area north-east of Lake Temagami.

Net Lake, east shore of, near north end ; S 4" W

Loon Lake, south end of S 3" W

Ko-ko-ko Lake, east shore of, i mile north of outlet S 18" W

{S 2" V
s vw

138 I

NIPI88ING AND TEMISCAMINO REGION.

T^iHt of Tetapaga Lake, north shore of, 1 mile eaut of outlet S 1° W

Htrie- CojK. Turtle Lake, north Hhore of {s 26° W

v.'

Vermilion Lake.

-f

■

s
s
s

"IS

Island in Vermilion Lake, A mile so>ith-\vest from north-east end. . S

Turtle Lake, small island near north sliure of

Waibikaiginaising Lake, island near east shore of, 3 miles from J
south end

East end of portage between Summit and Friday lakes

Friday Lake, west shore of, IJ miles north of outlet. .
Bear Lake, east shore of, 2 miles north of outlet

10^ W
15- \V
30° W
52^ W

!t°E
29° E

8°E
18^ E

f)°E
16= E

4°W

8° W

Wickstead (or Shabosaging) Lake.

On rocky islets, 1 J miles south-west of inlet

On south-east shore, IJ miles so\Uh-west of inlet
On north-west shore, 2 miles south-west of inlet.
On Rocky islet, 4J miles south-west of inlet

At Narrows, 2^ miles north-east of outlet

On islet near west shore, 4^ miles south-west of inlet

On islet near west shore of big western bay, 4 miles south-west of inlet
On west shore, 1 mile north-east of outlet

Annima-nipissing Lake and vicinity.

West shore of bay on route to Mountain Lake

t S 14° W
\S27°W
S27°W
S 240 W
S 27" W.
f S 14° W
I S 24' W
/S24 W
IS34^W
fSlSPW
\S24' W
/ S 23° W
(.S3rW

Island near centre of lake, 4 miles from north end . - ^

(Jull Rock Lake, north-east shore S

Carrying Lake, south shore of - o

Diabase Lake, south shore of - u

West shore, 3i miles from north end

10° E
2°E
3° W
(i° W

37° W
!»° W

20° W

29° W

20° W
7°W

20° W
3°W

18° W

Rabbit Lake and vicinity.

f S 1° W
Rfibbit Chute on Matabitchouan River, at outlet of lake -^ a g° w

West side, i mile south of Rabbit Chute S 3° W

rs 3°w

Is 8° W
Burnt Point, on west side of south end of Outlet Bay -I u 330 -^y

Is 38° W

South-east shore, 1 mile north-east of Rabbit Point S 13° W

/-S 2°W

I S 13° W
Point on east shore, i mile north of Rabbit Point -! ^ 3.0 -^y

U 42° W

»*«"'«'] ECONOMIC GEOLOGV. 139 I

iHland in Rabbit Lake, op|)o.site Rabbit Point 9 "fi^^W List nf

rS 4' W striie— Cont.

RosH Lake, soiith shore of <H 22", W

(.S 2'J'.\V

White Bear Point, on west shore \Vhite Btar Lake S 3',W

IhIs '1 in Wiiite Bear Lake, near north-east corner -^ S lo'^W

ts 40^.W

Montreal River and vicinity.

South end of Mountain or Round Lake S 42' E

On islet in river, 1 mile below Mud Lake portage S 22^ pj

At Fountain Falls S 17° E

Ii^land near west shore, near north end of Sharp Lake S 40' \V

ECONOMIC GEOLOGY.
Gold and Silver.

Throughout the whole of the large area coloured as Laurentian on (fold and
the accompanying map-sheets, very coarse aggregates of quartz and "
felspar with more or less mica, known as pegmatites, are of frequent
and often rather extensive occurrence. In origin they are distinctly
igneous and intrusive and in many localities are dyke-like, often branch-
ing and cutting across the foliation of the gneissic rocks, although in
other instances they occur as coarse-grained bands or belts interfoliated
with the finer grained granite-gneisses. These acid bands sometimes
become finer grained and not infrequently shade imperceptibly into the
mass of the gneisses with which they are associated.

Early in 1887 the town of Mattawa was startled by the report of Reported dis-
the discovery of gold in considerable quantity in a large number of [^ peginatites.
these quartzo-felspathic masses cutting the gneissic rocks in the
immediate vicinity. An examination was undertaken of these so-called
gold-bearing quartz-veins, and a number of samples taken to represent
nine of the principal localities were submitted to Dr. Hoffmann, Chemist
and Mineralogist to the Survey, which when assayed furnished only
negative results in the case of both gold and silver. The following
table shows in a concise manner the results thus obtained* : —

Locality.

Description.

Mattawa, hill on north side
Ottawa River.

Hill on east side

River 3 miles north

Mattawa.
3 miles west of Mattawa and

A mile north of McCool's

miU.

Quartz and felspar (pegma-
tite) large samples from
five different localities. .
Ottawa Quartz and felsjiar in mica
schist.

Quartz with a little felspar.
Large sani pies from three
different localities.

Gold.

None
None
None

Silver.

None
None
None

I ! M i

!i '

♦Annual Report, Geol. Surv. Can., vol. III. (N.S.), 1887-88, pp. 30-31
Assays Nos. 22-30.

I HIM

lliii

:'JiJ

140 I

NIFISSINO AND TEMI8CAMINU HKGION.

(Quartz

v*'iiiH Lac des

Quinze.

About the same time, samples from apparently sejjregated veins of
(juartz, containinj^ more or less disseminated sulj)hides and cuttinj^ what
has been mapped as Laurentian gnoi?s in the Lac des Quinze region,
were obtained by Mr. C. C Farr of Haileybury, Unt. These were sent
to the Geological Survey and handed to Dr. Hoifmann whose assays
showed only traces of the precious metals. The following table con-
densed from Dr. Hoffmann's repoit will show the result of his exami-
nations ami assays* : —

Locality.

DeHcrij)tion of Sjiecinien.

Weight

14 oz.

4h "

8 ..

Gol.l
per ton.

.Silver
per ton.

Route to Abitibi, 8 miles S.

Height-of-liiiul.
R. A. Klocks liiiiiit, north

sliore Fjiic (If.s (Quinze.
Lac den (2">"ze, north-east

end.

Chalcopyrite and quartz.

Pyriti^ .and pyrrhotite and

(luartz.
Pyrite in (piartz with ferric

hydrate.

Trace

II
M

None
Trace

Quartz aHsay.s, In addition to these, samples of cjuartz containing in some case pyri-
Nipis.sing and ^^^ material were sent to the Director of the Geological Survey, but
vicinity. their assays by Dr. Hoffmann did not afford any encouraging results as

far as regards their gold and silver contents. These samples were from
Lake Nipissing and the region adjacent and the results of their exami-
nation in the laboratory of the Survey may be referred to as
followst : —

Locality.

Description of Specimen.

Weight.

Gold I Silver
per ton. 'per ton.

Sturgeon R. (branch of) N.
of Badgerow Tp.

Small island in Lake Nipis-
sing.

Vein crossing inlet, W. end

Lake Nipissing.
Great Manitou Island, Lake

Nii)issing.
TwonnlesW.N.W.ofN

Bay.

Finelv crystalline galena and
cfialcoi)yrite with a little
(juartz.

Chlorite-schist, inica-schi^t,
gneiss and calcite with a
little pyrrhotite and py-
rite.

Rust-stained quartz & gneiss.

Felspar and quartz with nio-
I lybdenite and pyrite.
North] Rust-stained quartz with py-
rite.

(52 oz.

8 t,

i -1
4i lbs.

very dis

tinct

traces.

15 ■ 75 oz.

■IIG .,

Character of In the area characterized by the presence of Huronian rocks and
oniaii rocks, their associated eruptives, a large quantity of whitish or grayish

♦Annual Rei^rt, Geol. Surv. Can., vol. III. (N. S.), 1887-88, part T, analyses
Nos. 11-13.

fAnnual Reix)rt, Geol. Surv. Can., vol. II. (N. S.), 1886, part t, analyses Nos.
53. Vol. IV. (N. S.), 1888-89, part h, analyses Nos. 82, 84 and 86.

■ARkOW

]

ECONOMIC GEOLOGY.

141 I

foiinrl in them.

translucent quartz h an almost invariable accompaniment of any
extended exposure of rock. This cjuartz is seen to represent segregations
of secondary silica filling in the various cracks and fissures caused by
the profound orograpliic movements through which these strata liave
passed. Sometimes this vein-quartz is in the form of lenses or eyes
occupying various small gaps or openings in the rocks, these gradually
increasing in size until lenticular masses of ([uartz of considerabledimeu-
sions are formed. In some cases these masses run for considerable dis-
tal 1^' approximate in character to true fissure veins, although large
am, J jiical examples of such veins are exceedingly rare in this region.
Both in their horizontal and vertical extensions these " gash-veins "
are exceedingly irregular, and in no case noticed can any great
reliance be placed on their persistence in any direction. Calcite and
dolomite often occur in association with the quartz of such veins, with
varying quantities of pyrite, chalcopyrite and galena ; while sphalerite
and hiematite (micaceous iron ore) are occasional constituents. The
quartz is very often more or less cavernous or cellular, owing to the ox-
idation and partial removal of the sulphides originally present. Where
pyrite has been abundant the quartz is more or less rusty, while the
various cavities are partially filled with ochreous material. On the
other hand, where copper-pyrites is the more abundant, the quartz is
more or less stained and coated with green and blue carbonates of
copf Occasionally the galena shows a thin coating of carbonate
of ?erussite) where exposed to atmospheric action, and Dr.
Hoflfmann makes a note of its occurrence at the Macinac lead-vein on
Haycock's location, east side of Lady Evelyn Lake, one and a quarter
miles south of the outlet.*

In origin, many of these quartz veins, and especially the larger ones, '|'i,^.jp origin
are connected with the eruption of the large masses of diabase and
granite that invade the stratified slaty rocks, and often they are either
on the line of junction between these two rocks or occupying breaks
and fissures in its immediate vicinity, produced during the eruption
of these igneous rocks. Occasionally, such secondary veins of quartz
occur in irregular fissures in the diabase itself.

Some of the most important of such veins noticed, occur on the ,r •

_ _ •^ Veins on

" Mattawapiki," as the last stretch of Lady Evelyn Lake before Lady E^Nclyn
reaching the Montreal River, is called. The western shore of this * *^'
portion of the lake is composed of diabase, that rises abruptly from
the surface of the water and often from steeply sloping or perpendicular
clifis. The contact between this rock and the slates is concealed for

* Annual Report, Geol. Surv. Can., vol. IV. (N.S.), 1888-89, part r, analysia
No. 60.

ir 1

I r

£S'.:i:M

'{I jj

^ii^

Haycock
location.

.\!says.

142 I

NI PISSING AND TEMISCAMING REOToN.

the most part by the lake, the eastern shore being altogether composed
of a very distinctly banded greenish slate, which also rises into rather
important elevations, having apparently been protected to a consider-
able extent from denudation by the proximity of the more unyielding
diabase. The contact, for a short distance, runs inland along the
western shore, leaving a comparatively narrow strip composed of the
slates, which are seen to have lieen much shatterea and broken up liy
the intrusion of the diabase. Some considerable masses of segregated
quartz were here noticed filling irre'^ular cavities and fissures
produced during the eruption. Associated with the quartz is more or
less calcite, and in this gangue were noticed galena, copper-pyrites,
iron-pyrites and zinc-blende. The banded slates on the eastern shore
dip in an easterly direction at an ani,'le of about 18°, and
associated with and cutting these are similar segregated masses or
" gash-vein," in which galena is the prevailing constituent. The
property on which these veins are situated is owned by Messrs. Klock
and Haycock, and is locally known as the Haycock mine or location.
A considerable amount of development work has been done, looking
chiefly to testing th.e quality and extent of the ore-bodies, but the
inaccessability of the locality would be a sufficient hinderance to any
further operations, unless the deposit should prove of an exceptionally
rich character. Assays of representative samples from these and
similar veins exposed in the immediate neighbourhood, have been
made in the laboratory of the Survey, which may be summarized as
follows* : —

Locality.

Description of Specimen.

Weight.
1 lb. ooz.

Gold
prton.

Silver
per ton.

W. side Lady Evelyn Lake,

Quartz v.ith a little calcite

Traces

204

near outlet.

and chalcopyrite

K. side Lady P]velvn Lake,

(laleiia with a little quart/.

6ibB. 12oi:.

875oz.

1:^ nnles S. of outlet.

and calcite.

\V. side Lady Evelyn Lake,

Quartz with a little chalcopy-

2 lbs.

None.

OllToz.

14 miles tS. of t)utlet (north

rite, galena and zinc blende

W. side Lady Evelyn Lake,

Quartz vatli chalcopvrite

2 lbs.

None.

H miles S. of outlet (south

vein).

W. side outlet Lady Evelyn

(Juartzwithcalcite.dolomite,

1 lb. 12 oz.

Lake (west vein).

serpentine and chalcopyrite

Island at Narrows, 3 miles S.

Quartz with chlorite

13 oz.

of outlet of Lady Evelyn L

Oocklinrn

The Cockburn location or mine covers several small islands in

location, Cross
Lake.

Cross Lake, near the inlet from Temagami Lake. On these islands,

•Annual ReiKirt, Geol. Surv. Can., vol. IV. (N. 3.), 1888-89, imrtit, analyses Nos
m-VA.

•ARLOW.

]

ECONOMIC GEOLOGY.

143 I

several masses of segregated quartz are exposed, but these apparently
have no great regularity or persistence. The largest of these so-called
veins is situated on the west side of an island about a quarter of a
mile in length, about half a mile south-west of Temagami River. The
island is composed of a greenish-gray, greywacke, slaty in structure^
which has undergone considerable alteration, and sericite is rather
abundantly developed, especially on the planes of cleavage. The
pressure or foliation planes, which are here apparently the only
structural features displayed by these rocks, have a strike N. UV E.,
and an inclination eastwards <7V. The quartz fills an irregular
fissure in the slates, is about five feet in width, has a strike of N . 38' E.,
and nn underlie towards the south-west <45°. Galena, iron-pyrites,
copper- pyrites and malachite were all noticed imbedded in the quartz.
Samples taken to represent the average of these were examined in the Assays.
laboratory of Survey with the following results* : —

Locality.

Island in Cross Lake iiear

outlet

Cross Lake

Cross Lake (same loc. as last)

Description of Specimen. Weight.

Quartz with galena and chal-

copyrite

Quartz with chalcopyrite . . .
Quartz with galena

lb. oz.

1 10

Gold
per ton.

none

.058oz.

trace

Silver
per ton.

•175oz.

•0.58OZ.

2:i.3;ttoz.

Mr. p. A. Ferguson of Mattawa owns three mines or locations on Fergvistui loca-
Lake Temagami, known respectively a^ A, B and C. At location A, Temagami.
situated on the east side of Sandy Inlet in the northern part of the
lake, the rook is for the most part a massive dark-green medium- textured
diabast, much of which is broken up ; the irregular cavities being filled
with quurtz and calcite, with which are associated yellow epidote and
small dodectedral crystals red garnet. One of the veins from which
considerable Material had been taken was noticed near the water's edge
and contains in. addition to the minerals mentioned above, a little
iron-pyrites and copper-pyrites. The vein is very irregular and only
about a foot in width and thus too small to constitute a workable deposit.
At location B, situated on the north shore of the north-east arm of
Lake Temagami, about two miles east of the portage into Caribou Lake,
the rock is a pearly grayish-green sericite-schist, striking N. C8" E. and
dipping northwards <70\ Associated with this is a lenticular mass
of light-gray rusty weathering dolomite, containing reticulating veins
of quartz, that stand out on weathered surfaces. Chiefly at the contact
between these two rocks, is a considerable deposit of iron-pyrites,

*See Annual Report, lieol. Surv. Can., vol. IV. (N. S.), 1888-89, jmrt u,
analyses Nos. 54, 57 nnd 58.

i 'M! !

I ' I

^^m

144 I

NIPISSING AND TEMISCAMING REGION.

i '

AMsays.

Veins on
I)('n«hi«
Island, Lake
'rt'inaKiinii.

Assays

Veins on

TeniaKanii

iMlanu.

with a little copper-pyrites and arsenopyrite (1) Location C, is on an
island now known as Ferguson Island, to the south-west of this point
and consists of iron-pyrites in association with sericite schists.

Assays of specimens taken as representative of these three deposits,
ffave the following results in the laboratory of the Survey* : —

Locality.

Description of Specimen.

Weight.

(Jold

Silver

per ton.

(ler ton.

Ferfrnson Location A, Sandy

(Juart/. with little pvrite and

Inlet fi. Tcniapann

chalcom'rite

lllbs.

trace

Ferffuson Location B, north

(inart/. with finely disseniin-

east Ann L. Teniajranii.

ated pvrito

filbs.

none

.2330Z.

Ferguson Location C, Is'd. in

Rust-stained sericite schist

N.E. Arm L. Teniagaini

with i)yrite

15o/..

trace

•II60J!.

The Denedus Islands near the entrance to M uddy- water Bay on Lake
Tomagami, and so-called after a well-known member of the Temagami
band of Indians, is another mining location, owned by Mr. James
Holditch of Sturgeon Falls On the two large islands composing this
group, the rock is a dark greenish-gray felspathic sandstone or grey-
wacko, sometimes slaty in structure but usually massive. The rock is
much broken up in places, and the irregular cracks and cavities thus
formed are filled with gray translucent quartz, with which is usually
associated more or less pinkish dolomite. Occasionally these fissures
are so large as to include considerable masses of quartz On the west
island a quartz vein about two feet in width, occurs with a south-
easterly strike containing both iron- and copper-pyrites. A some-
what larger segregated mass of quartz occurs on the island to the east,
with similarly disseminated grains and fragments of iron- and copper-
pyrites and occasionally a little galena. Assays of specimens from both
these islands were made in the laboratory of the Survey with the follow-
ing resultst : —

Locality.

Denedus Islands (east vein).
Denedus Islands (west vein).

Description of Specimen.

(Quartz with a littlt^ chlorite
and dolomite

Quartz with chlorite chal-
copyrite and pyrite

Weight.

(4old
l>er ttm.

lbs. oz.

2 (>

none

» C

trace

Silver
jwr ton.

none
trace

Large masses of iron-pyrites, associated with pyrrhotite, copper,
pyrites and magnetite, occur on the east side of Temagami Island in

•Annual Rei^rt, Geol. Surv. Can., vol. IV. (N. S.), 1888-89, part K, analyses
Nos. (i9-7L

fAnnual Report, (!eol. Surv. Can., vol, IV. (N. S.), 1888-89, jiart H, analyses
NoH. 79-80.

i 'i

ECONOMIC GEOLOGY.

145 I

Lake Tt'inagami and on the south-east shore of YermiHon Lake, to
the nortli of the north-east Arm of Lake Teniaijami. Samples of these
were assayed for goUl and silver, but with negative results in both
cases. Subse(]ueiitly Mr. E. V. Wright, who had located the Vermi-
lion Lake property had the ore assayed for nickel, but less than one per
cent of this metal was found. The follovviny; statement yivesthe results
of the assays made* : — As.siiya.

T.doiilitv.

Di'scription of Siiec'inion. NVeight.i HoUl

! iiwr tim.

'rt'iiiiiKatiii Is"(l. (('list sin >ro). i I'y rite, clialco|)yriti', iimgue-; j

i titt', «itli cliloritc 4 2 | iiinif

N't'niiilioii Livkc I'yiittMii clilDritc-.scliist imil; i

([iiartzito I 13 "

Silver
per toil.

Ill

On Matthias Island, about two miles north-east of the Hudson's 15ay On Muttliiiis
Co.'s post on Bear Island in Lake Temagami, a (juartz vein with a S(ime-
what uniform width of about eight feet was noticed. The quartz is
white and translucent, filled with rusty cavities and a little copper-
pyrites, ii'on-pyrites, malachite and aidverite were noticed Although
80 promising in appearance, assays made in the laboratory of the Sur-
vey show neither gold nor silver, f

At the (.uay mine, in rear of the Township of Fabre, on the east <!<iii.v mino.
side of Lake Temiseaming, according to Mr. J. Obalski, of Quebec;, a
considerable amount of copper-pyrites has been found. This, associ-
ated with and disseminated through diabase, probably an extension
eastward of the mass which reaches Lake Temiseaming at Quinn
Point, shows on assay according to Mr. Obalski, gold, "02 oz., and
silver, I'aG oz. per ton of 2000 lbs.

Other specimens examined in the laboratory of the Survey during Ons assiiyod
the progress of the exploration, from veins and masses of quartz that i^'j!||jf •','.'.'""'*

•Annual Reiwrt, (Jcol. Surv. Can., vol. IV". (X. S.) IHHS-.SII, I'art K, analyses Nos.
7S mill 52.

|.\nniial Ki'iiort, (ieol. Surv. Can., vol. IV. (X.S.), ISS.S Sit, Part it, analysis
No. 53.

146 I

NIPISSIXr. AM) TKMIiSCAMlNO HKGION.

are of less importance either on account of the negative or small
results obtained, or the liinited extent of the masses themselves, are
enumerated below* : —

Locality

N. end of Lake Tumaganii .

Pyrite in quartz and calcite

'(fiol" 10 ft. vein).
(Jrayisli oi)ai|iie quartz with

a little (lyiite.
Quartz witli a little chlorite

ivnd cliak'(i|iyrite.

Little Kiver. 1 mile Yj. Lake

Temiscaniiiif,'.
Point K. of outlet Hay Lake,

N.-E. arm Lake Tenia^'anii
N. .'iliore, N.-E. arm, ■/ mile, Quartz with traces of iron

W. portage, Lake Tema-l and copper.

ganii.
Montreal River, (5 miles from Red and white quartz with a

mouth. I little elialcopyrite,

E. shore l''<>rt'usonT3ay, Lako'Cak'ite with a little chlorite

Tem;igaini. I and elialcopyrite.

Small islet in Wliitefish Bay, (Quartz with jiyrite in fels

Lake Teniagami. | jiathic sandston(>.

Islet ij mile AV . of Temaganiiitjuartz with a little dolomite

Po>t. and chlorite.

Twt) miles N.-\V. of Tema- ( hiartz with chlorite and a

gami Post.
Island neai' S. end S.-W.

arm Lake Teniagami.
Mountain Lake, ^Montreal

River.

Portage near S. end of Lake
Temagami.

Island Ij miles N.-E. Tema-
gami Post.

little pyrite.

Rust-stained quartz with a
little ))yrite.

Rust-stained quartz with py-
rite and elialcopyrite in
diabase.

CJuartz with chlorite and
dolomite.

Rust-stained quartz with a
little ilmenite.

:we

ght.

lbs.

■I

Tri'ce I None.

I
I
None I II

Trace l'2!)0oz.

I
None liNone.

Distinct! n
trace. I
None ! II
I

Ti-ace i Trace.

Ni )ne i None.

Trace

None
Trace

Trace.
None.

little explor
ation as yet.

Comparatively Although the results given in the above tables are not very encourag-
ing, it must be remembered that the assays were made from material
obtained during the progress of an exploration over a wide stretch of
country in which only limited opportunities were aifoi-ded for exfimina-
tion and selection while only those quartz masses were visited which were
noticed exposed at or near the shores of lakes embraced by the survey
or in localities otherwise accessible. No systematic attempt has ever
been made at prospecting throughout the greater portion of the dis-
trict, although a few enterprising individuals have looked over part of
the area in the hope of finding some unusually rich mineral deposit.
A large portion of the area covered by the Huronian rocks in the
north-western part of the region, is thickly covered bj' forest, composed
chieily of evergreens, which conceals much of the surface, rendering

*Annual Report, (Jeol. .Surv. Can., vol. III. (N. S.), 1S87-H8, i)art T, analysis
No. 32.

fAnnual Report, (Jeol.Sinv. Can., vol. IV. (N. S.), 18.S8-89, part K, analyses Nos.
10, 72, 73, 75, 77, 05, 07, 08. 87 81 (iij

•]

ECONOMIC GEOLOGY.

147 I

any attempt at prospecting difficult. The inaccessibility of the region
has also generall)- prevented any extended examination by prospectors,
but the recent survey of the Nipissing and James Ray railway and the
proposal to run this line northward from North JJiy to the east end
of Lake Temai,'ami, has again drawn attention to this region as a
promising mining field. The Huronian bolt of rocks is tiie same that Coiiditions
traverses the Sudbury mining district to the soutli-west, while similar yii-'jiju'ly' '^''
associations of slate and greyvvacke broken tlirough by diabase, gabl)ro
and granitic intrusions, furnish conditions eijually favouraVile to the
presence of metalliferous snlphides or gold-bearing quartz-masses now
known to exist in the vicinity of Wahnapitae Lake, immediately adjoin-
ing the Temiscaming sheet to the south-west.

One of the most important of the mineral deposits in this district, Wiight mines
both on account of it-; comparative accessibility and the character and ^'^^y 'iVinis-
size of the ore-bearing body, is wliat has usually been known as the
Lake Temiscaming silver or lead mine (Wright's mine) comprising
portions of lots 61, 62 and 63 of range I., in the Township of Duha-
mel, in what are called Blocks A and B, on the east shore of Lake
Temiscaming.

Although, this deposit was brought to notice by Mr. E. V. Wright, of Discovery,
Ottawa in 1877, the existence of ore at this place was known long
before, for on a " Map of North America,"* based on D'Anville's map,
and published about 1778, the small bay on which it is situated is
named " Anse a la Mine."

In the vicinity of the mine, the rock is the breccia-conglomerate form. Association.
ing the basa! member of the Huronian in this district, the pebbles or
fragments of which are chiefly of granite, diabase or other eruptive
rocks, embedded in a greenish, chloritic, slaty matrix, which owing to
pressure appears to curve around or enfold the inclosed fragments.

The deposit occurs in a brecciated or shattered belt of the rock, ch.iiactcr
composed of angular or subangular fragments, the interstices being of deposit,
filled by galena with occasif)nally a small quantity of iron-pyrites
together with more or less pink dolomite. Although this zone is about
eighty feet in breadth and contains a varying quantity of galena
throughout, only about six feet can be said to carry the mineral in
workaVjle quantity, and even this with considerable admixture of gan-
gue and rocky matter. The rock immediately adjoining and inclosing
the deposit, has a decidedly porphyritic appearance, crystals and frag,
raents of white felspar and grains of transparent quartz being embed-
ded in a fine-grained greenish matrix. Under the microscope, this fine.

*See Map No. 5, Mills' Reixirt ou Boundaries of Ontario, Toront<j, 1873.

10^

; :

, I.

l! :ii

;,S

US 1

NIPISSING AND TEMISCAMING REGION.

grained groundniass is seen to be composed of finely granulated quartz
and felspar together with a considert^ble quantity of chlorite and seri-
cite in fine scales. Through this are scattered the larger fragments
which are apparent to the eye. Some of these are composite fragments
of Eome porphyritic rock, with large crystals of well striated plagiocla.se
anc' firiely granulated (quartz. Whilst the majority of the quartz-frag-
ments bear evidence of hi ving been subjected to considerable pressure
one large subangular graiii extinguishes very evenly and shows little
or no trace of disturbance, The plagioclase individuals have a broad
tabular habit, are well striated, very turbid, and apparently constitute
the predominant felspar, although unstriated felspar was observed.
Ilmenite, accompanied by leucoxene, is rather plentiful, some of it
is entirely altered to the latter mineral.

Assays. Samples of the ore were sent to the Geological Survey in 1877, and

Dr. B. J. Harrington states* that a specimen of the galena entirely free
from gangue, gave, by scorification, silver 18-958 ounces to the ton of
2000 lbs. Another specimen received about the same time, but con-
taining a good deal of rocky matter, gave, silver 11 '06 ounces to the
ton, while a third specimen taken about fifty feet from the aljove gave,
after careful separation of the gangue, silver 18'229 ounces to the ton.
The mean of two assays by Dr. Hoffmann gave, silver 13'f38 ounces to
the ton with a trace of gold ; by Prof. J. T. Donald of Montreal, silver
.~i?21.17 ; iiy Dr. Baptie of Ottawa, silver 2-3 ounces ; by School of Mines,
London, 13 oz. 14 dwt. 10 grs. per ton of 2210 lbs. and lead 52
per cent. The percentage of silver in the galena itself was 26 oz. 7
dwt. 21 grs.

Average silver The silver content of the pure galena would therefore seem to vary
content. ^^.^^^^ 18 to 24 ounces to the ton of 2000 lbs., but the large intermixture

of locky matter would considerably lessen these results. Iron-pyrites
has been found intimately associated with the galena, and occasionally
considerable quantities have been encountered in working the deposit.
This is doubtless the source of the gold usually present in the ore.

Exploratory
work.

Work was begun on this deposit in 1887, under the management and
ownership of Mr. E. V. Wright, of Ottawa, but only preliminary develop-
ment work was undertaken. During 1888, however, work was carried
on very energetically, and a shaft was sunk to the depth of about 100
feet, while concentrating machinery was set up and it was proposed to
smelt the ore on the spot. Various obstacles have stood in the way of
the successful development of this mine, chief of which has always ben

main line o

Report of Progress, Geol. Surv. Can., 1877-78, pp. 51-r)2.

•J

ECONOMIC flEOLOOY.

149 I

its distance from railway coirimunication and the consequent difficul-
ties in shipment of ore or concentrates.

For several years work went on in a rather desultory fashion, but in
1890 the Mattawa Mining and Smelting Co. of New York, took hold
of the property and an extensive and costly plant for the proper hand-
ling of the ore was installed. The main .shaft was increased in depth
to over 100 feet, and two drifts were made to prove the extent of the
deposit, while a diamond-drill boring carried to a further depth of 75
feet, proved the existence of the galena to a total depth of 140 feet.
Operations were carried on energetically till March, 1891, when work
was suspended. During the summer of 189G, work was again resumed,
chiefly with a view of further testing the property and it is hoped that
the recent completion of the branch line of the Canadian Pacific Rail-
way to the foot of Lake Temiscaming may lead to continuous working.
The main shaft is now sunk to a depth of nearly 200 feet, and it is
reported the mineral shows no diminution in either quantity or silver
content.

Nickel, Copper, Etc.

i^:.''!

The Huronian belt of rocks, characterized by the presence of great Ores contain-
deposits of nickeliferous and cupriferous ores in the Sudbury district, "j^*''] l!^,!)',,^".' ^
runs with unbroken c>mtinuity through the Temaganii and Temiscam- pyi'it««-
ing districts. Diabases and gabbros apparently identical in their com-
position and appearance are present over large areas, but so far no very
large deposits of pyrrhotite and copper-pyrites have been found. On
the west side of Tema;;ami Island, as well as on the south-east shore
of Vermilion Lake, considerable masses of these sulphides are present,
but the assays made show only a very small percentage of nickel.
Copper-pyrites is an almost invariable constituent of the diabasic
masses and in places pyrrhotite is equally abundant, and it is highly
probable that systematic prospecting may develop large deposits con-
taining nickel and copper.

At the Guay mine, in rear of the Township of Fabre, the specimens
of copper-pyrites gave, according to Mr. Obalski, 72 per cent of
copper, and -OS per cent of nickel.

The inaccessibility of the region, however, and the abundance of
these nickel and copper bearing sulphides in close proximity to the
main line of the Canadian Pacific Railway, in the Sudbury mining dis-
trict, many excellent deposits of which have not yet been developed,
prevent any extended search in the Temagami and the Temiscaming
districts.

!ii I

I f

I \

150 I

NIPISSIJrO AND TEMI8CAMING REGION.

oil.

OcourriTicc.s
of iron ore.

At Ket'pcwa
Lake.

On Iron
Island, Luke
Ni pissing.

Ore not
abundant.

No depcsits of iron ore of economic importance have as yet been
found in tins district, although both niaj,'netite and hannatite are ratlier
abundantly di.stributetl. Wherever nuticed, the (juantity has been
too insignificant, or the as.sociati(jns tiucii that the material seen could
not be utilized with any degree of profit. Magnetite occurs in patches
and small masses in the red granitoid-gneiss exposed in the neighbour-
hood of the Chute des Paresseux vi\ the Mattawa, in the township of
Olrig. On the west side of Keepawa Lake, a short distance north-west
of Cordon Creek outlet, a dark-gray gneiss containing a consider,
able proportion of magnetic iron ore occurs, and a (juantity of this ore
was mined and taken to the Wright mine on Lake Temiscaraing for
use as a ilux in the smelting of the galena. The ore, however, is too
lean and silicious to be of commercial importance.

On Iron Island, according to Mr. Murray,* " small masses of specular
iron ore are common to most of the rock in the island and in the crys-
talline limestone, there is a very great display of it. For a breadth of
about forty yards along the cliil on t'ie east side, the rock holds masses
of the ore of various sizes, sometimes running in strings of an inch thick
or upwards, elsewhere and at other times accumulating in huge lumps,
someof which probably weigh over half a ton. Thebeach near the outcrop
is strewed with masses of all sizes, from great boulders weighing several
hundred pounds to small rounded pebbles not bigger than marbles. The
limestone with which the iron-ore is associated is frequently cavernous,
and the crevices and smallerfissuresare thickly lined with crystals of blue
fluoispar and red sulphate of barytes or cockscomb-spar. Crystalline
limestone crops out on the opposite or west side of the island, and, judg-
ing by the strike of the north side, it must correspond with that holding
the iron-ore on the east. The same minerals were found disseminated
thi'ough the rock and strewed upon the beach. At the extreme south-
west point of the island the rock is again crystalline limestone, and a
long leach running out from it to the westward is perfectly covered
with I)oulders of specular iron-ore. Iron-ore occurs also at the south-
east point of the island, although not in such great abundance and
only in detached masses strewed upon the beach."

Several parties have searched rather thoroughly over this island and
most, if not all, of the iron has been carried off and shipped away.
The interior of the island is a veritable jungle, and the shore is lined
with an almost impenetrable thicket of scrubby cedar. Several small
pits were noticed which had been sunk near the north-east corner of

*Keport of Progress, Geol. Surv. Can., 1853-50, p. 123.

magnetic r

•]

ECONOMIC GEOLOGT.

151 I

the island, l)ut the amount of ore s' cured apparently did not warrant
any further outlay of time or money, and it seeuis pretty certain that
this ore is nowhere present in workable (juantity. At the time ot the
writer's visit early in the spring most of the beach was submerged.

Magnetic iron-ore, interlaminated with bands of red, gray or black
silicious, .slaty rock was noticed in several localities, and in such con-
siderable (juantity as to constitute depcsits of workable size, but the
abundance of intermixed silicious matter is probably such as to render
them practically valueless. One of these deposits is situated on the
south-eastern end of a group of three islands near the eastern shore,
about three miles from the southern extremity of the South-west Arm
of Lake Temugami. The exposure seen consisted of alternate bands of
light- and dark-gray quartzite^, the dark bands being composed almost
wholly of grains of magnetite. It is curiously contorted, but has in
general a dip N. 7" K. <45°. In immediate contact with this to the
south, is a band of disintegrating greywacke and chlorite schist, dip-
ping N. 9° E. < 55°. This is tilled with pyrite, which has evidently
been the chief cause «)f its decomposition. The local attraction of the
magnetic needle was so great at this point as to render the compass
practically useless.

Near the west end of Tui'tle Lake, to the north of the north-east
arm of Lake Temagami, there is a somewhat similar deposit, consisting
of alternating reddish and black bands of hanuatite or jaspery iron ore
and magnetite, with some olive-green shale. The strike of the deposit
accords with that of the sericite-sehists in the immediate vicinity,
being N. 74° E. with a dip northwards < 70. In this neighbour-
hood also the compass was much affected.

A third locality in which magnetite in similar association occurs, is
on the Quinze River, on the tenth portage from Like Temiscaming. Mr.
W. McOuat thus describes the deposit : *" The portage is on the south,
or left hand side of the river, running in a direction about south-east
to a small lake in a narrow ravine, and is not more than a quarter of
a mile long. The iron ore crosses the portage near the upper or south
end. It occurs in the form of layers from the thickness of paper to
about an inch, and is interlaminated with similar layers of whitish,
gray and dull-red fine-grained quartzite. The iron-ore constitutes prob
ably from a fourth to a third of the whole, and as the thickness of the
whole band is about thirty feet, the whole thickness of the layers of
iron ore would probably not be less than eight feet. The band was
traced along the strike for about a hundi-ed yards. Magnetic oxydeof

'■ Re|)oit of Pr()gre.s», (ieol. Surv. Can., 1872-73, p. 131-132.

Iron nil
couth-west
arm, Lake
Teinagaini .

On Turtle
Lake.

On < Quinze
River.

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152 I

NIPI8SING AND TEMISCAMINO HKCilON.

m \

iron was observed under similar conditions at several points on this
portage, and on the next above, but in much smaller quantity."

On Vermilion Magnetic iron ore also occurs, but mixed with sulphides, on the
* ''■ south-east shore of Vermilion Lake and on the east shore of Teniagami

Island, in Temagami Lake. HiiMuatite (as micaceous iron ore) occurs
as a rather common constituent of the many quartz veins cutting the
Huronian throughout the northern part of the area, but it has nowhere
been found in deposits of sufficient extent to be of economic value.

Occurronrc (if Although of no economic importance, it will be of inteiest in this
pertlihe'^' " '" connection to note here the presence of native iron imbedded in the
crevices of some specimens collected on Mr. McMeikin's farm, about 4^
miles east of Mattawa. This occurrence of native iron, to which Dr.
Hoffmann's attention was lirst drawn by ]Mr. 31. L. Droadbt-nt, was
observed in some specimens collected as samples of perthite and
araazon-stone on lot 7, con. B, of thj township of Cameron. The fol-
lowing is a description by Dr. Iloil'mann :

Description
byriJr. Huff
mann.

Analysis.

■"■"The perthite, consisting of interlaminated brownish-red to red-
dish-brown orthoclase, and reddish-white albite, contained here and
there inclusions of a grayish-black, massive, pebbly magnetite, partiallj'^
altered, manganiferous magnetite, affording a dark reddish brown
streak.

" Portions of the felspar showed marked signs of weathering, the albite
more especially being more or less kaolinized. Imbedded in the kao-
lin, also in the dark reddish-brown limonite in immediate proximity
to it, were observable numerous spherules of a steel-gray colour and
metallic lustre. These spherules varied greatly in "-^e, a few measur-
ing as much as a millimetre in diameter, the greater numbei-, however,
being of far smaller dimensions, and many of microscopic minuteness.
They were almost perfectly spherical in shape, strongly magnetic, very
hard, indenting and scratching a hardened steel mortar ; brittle, when
pulverized emit a distinct phosphoretted odour ; immersed in a solution
of cupric sulphate, become coated with a lilm of metallic copper.
They were readily attacked by hydrochloric acid with evolution of
hydrogen and a strong odour of phosphine, leaving an insoluble residue
consisting of light-brownish coloured spherules which on ignition
become perfectly white. These spherules, which form tl\e nuclei of the
metallic-looking grains, have, apparently, a concretionary structure.

" Mr. Johnston found the metallic spherules to have a specific gravity
at 15-5° C. of 7*257 and a composition as follows : —

* Annual Reiwrt, Geol. Surv. Can., vol. VI. (N.S.), 1892-93, p. 23 n.

■ARLOW.

I ECONOMIC nEOLOGY. ir)3 I

Iron 9045

Miuiffniicse 075

Nickel trace

Sulphur "j

l'lii>s|ihi)nin ^ iindet.

Organic nuittcrj

Insoluble, non-metallic, residue 7 '21)

tl.S-4()

■ \ /

LinieKtdiir
Lake Teui
earning.

"Cobalt and copper were sought for and found to be absent. He
fuumi the insoluble non-inetallic residue to contain 88'77 per cent of
silica, a little alumina and ferric o.xide — not estimated, a very small
quantity of lime and possibl}' some magnesia.

" This occurrence recalls to mind that observed by me in a specimen
of Iluronian quartzite from the north shore of St. Joseph Island, Lake
Huron, Ont.*

Limestone and Lime.

On Lake Temiscaming, the Niagara formation so abundantly
exposed on the islands and shores of its northern portion affords
an unfailing supply of excellei\t building stone, in blocks of large
dimensions if required, while its fine and even texture as well as its
colour recommend it strongly for such purposes. The Anglican church
at Haileybury, on the west side of Lake Temiscaming, is being wholly
constructed of material procured from exposures of this limestone on
the east shoi'e of Mann or Burnt Island. For purposes of making
quicklime, the more thinly bedded fossiliferous portions seem to be most
suitable as furnishing the purest and best lime with least expenditure
of fuel.

The Manitou Islands, in Lake Nipissing, especially Macdonald or On Lake
Little Manitou Island, have furnished limestone which was used to 'l*^''*'"^-
advantage during the construction of the Canadian Pacific Railway.
An excellent lime-kiln was noticed on Macdonald Island, which had
evidently been used extensively. To the east of Mattawa, and
between this place and Deux Rivieres, a good deal of lime has been
manufactured for local consumption, as also near the foot of Talon
Lake on the Mattawa River. In the former instance the various out-
liers of Trenton limestone have supplied the material, while in the
latter a band of crystalline limestone has been made use of by the
incoming settlers. This band of limestone would furnish a very pretty
serpentine marble or ophicalcite.

When calcined, the deposit of marl covering the greater portion of
the bottom of Emerald Lake to the west of the Opimika Narrows, on

IS-

Jll i

m
m

Trans. Royal Soc. Can., vol. VIII., sect. III., p. 3!), 1800.

:f '

l')i 1

NIPI.SSIN(i AND TKMISCAMINO HEOION.

Huilding
stones.

Lako Tciiii.^c.iiiiiii^', would furiiLsli ii iioarly puro and vt-ry wliito limo
well a(lii{)tufl for luoriar ami oIIkt purposes. For such purposes the marl
should bo inoulchnl into bricks which, after drying, may he Imrnt in a
kiln. It might also ho omployiHi for whitowashing farm and other

buildings.

Granite tind (ineix>t.

During tho construction of tho Canadian Pacific Railway, tho gray-
ish evenly foliated gneissic rocks, often easily procurable in large blocks,
were used for bridge-piers and culvert work with satisfactory results.
Many exposures capable of yielding both gneiss and granite of excel-
lent (juality mi'v Vie found at intiirvals along the lino of railway.

On Temis^ aing L; '.e, in the vicinity of Baie des Peres, there is a
very befiutiful deep llosh red granite, in which the more or less rcAinded
outlines of the disseminated grains and fragments of grayish translucent
quartz give the rock a fine conglomeratic or prophyritic aspect.
It is not known, however, whether this granite can be obtained sutdci-
ently fr'ce from joint's.

Throughout the entire area the frequent and large masses of griinite
exposed, as well as tho more massive and granitoid portion of the rocks
classified as Laurentian, would furnish building stones of good
quality, but only the more readily accessible localities of such rocks
can be supposed to possess any importance.

Flagstones and Slates.

Flags. The better qualities of slate do not occur extensively in this region,

but some portions of the strata constituting the slaty or middle mem-
ber of the Huronian, present very line-grained and fissile beds which
are firm and strong : although most of the specimens seen are rather
thick for I'oofing purposes. Search might reveal some localities where
suitable material occurs in sutHcient abundance to be of economic im-
portance. Many portions would however seem to be well adapted for
flagging.

On the east side of Lake Temiscaming between McMartin Point and
Latour's mills, the shore-line for several miles is formed of vertical cliffs
of very evenly banded or foliated micaceous gneiss. The layers are
extremely regular, fissile and of suitable thickness to yield flagstones
of the very best quality and of almost any size.

Litliographic Stone.

Lithographic Some of the finer-grained beds present in the Niagara outlier on
stone. Lake Temiscaming, exposed on Mann or Burnt Island as well as at

]

ECONOMIC OEOLOOT.

inr, I

Dawson (Wain) Point on the mainland to the north, exhibit portions
wiiich wore thought to be suitable for lithographio purposes. .Some
([uairying waa done on the west shore of Mann Islnnd, iit.fl
lately a company with heaihjuarters at Vankleek Hill comnu iu'wl
operations in the vicinity of J)awson Point with a view to yi-ouring
suitable material if possible. So far, however, the specimens ptocureil
are not sutlicicntly uniform in texture, but it is still pot^siblo that
litliographic stune of economic value may be discovered. Further
examination of theso beds with this object seems desirable.

t- v:

Felspar,

Although this mineral is abundantly distributed as one of the F.l^pir.
most iu)]iortaiit and characteristic constituc^nts of these crystalline
rocks, only a very small proportion is found pure enough antl in
sulKciently large masses as to be employed for industrial purposes. To
be of value, the deposits must be readily accessible and must con-
tain the mineral in large cleavable masses easily freed fi'om other
associated minerals or impurities by a rough cobbing before shipment.

There are many large pegmatite dykes close to the line of the Can-
adian Pacific Ptailway throughout this district, which might bo
examined with a view to obtaining supplies of felspar. Some of these
near Nosbonsing station seemed to furnish abundant and very suitable
material.

Felspar is chiefly employed in the manufacture of porcelain and
pottery.

Shell Marl.

Deposits of this kind are frequently found below accumulations of
peat, the marl in these instances being, therefore, 9l not very recent
formation, but in other cases it is found to be still in process of deposi-
tion, covering the bottoms of shallow ponds or lakes.

Emera' 1 T.ake, about five miles west of the Opimika Narr »ws, is at
tl head waters of one of the branches of Opimika Creek, which

■aches Lake Temiscaming from the west immediately above the
Opimika Na \vs. This creek, as well as the lakes which it empties,
are ' narkable for their clear water. Emerald Lake itself is corn-
pa: lively insignificant in size, being only about half a mile in length,
by a quarter of a mile in greatest width at the .southern end, gradu-
ally tapering towards its lUtlet at the north- rn exti'emity. The lake
is in a small valley from eighty to one hundred feet in depth. At the

Slipll mnrl
on Kiiii^ralel
L;.k-.

■ii

■ill.

■).;

i 1

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lira

156 I

NIPlSSlXil AND TEMISCAMING IIEGI05.

Analysis.

south-east corner is a very shallow bay, affording entrance to a stream
which is fed by a number of large cold springs that rise at the base
of an amphitheatre-like gully, at the base of steep banks composed
mainly of sand and gravel. The water of the bay, although so shallow,
is very cold even during the hottest days of summer, while the whole
bottom is covered witii a deposit of shell marl of unknown depth.
That tins depth is considerable there is no reason to doubt, as the
soundings made with long poles failed to reach the bottom of the deposit.
Besides this bay the whole lake contains marl deposited o.i the bottom,
while the pobljies and boulders near the outlet show a coiisidorabie
coating of this loosely coherent, earthy carbonate of lime. Tlie wa r
of these springs is evidently calcareous, and is found to be slightly
aperient.

According to Mr. J. F. Whiteaves, who has examined the speci-
mens of fresh water shells obtained from this locality, the species
represented are Sphceriwin snhatum (Lam.), and Planorhis trivolvis
(vSay) var. m.acrosto)nus (Wliiteaves).

A sample of the marl examined in the laboratory of the Survey was
found to liave the following composition* :- -

Hygroscopic viiter (iifter drying at 100' C). . I'Od per cut.

Lime tS ' 82 h

Magiu'sia 04 n

Aluiiiinr, 07 «

y<'rric' oxide O'OS n

Manir iHous oxide Traces

I'otassa Traces

Soda Traces

Carbonic acid liSOl h

Suli)Iun'ic acid 07 m

riiuspiit.ric acid 002 „

Silica, soluble 0" 10 n

Insoluble niiii(#al matter 8' 02 n

Organic matter, viz. ; vegetable fibre in a state of
decay, and products of its decay, such as hunuis,
liuuiic acid, etc., and ix)ssil)ly a little combined
water 4 ' 70 n

Total 10012 I.

" Assuming the whole of the lime to be present in the f,.irm of carbon-
ate, trilling quantities of which are, however, present in other forms of
com')ination, the amount found would correspond to 8G • 28 per cent
of carbonate of lime. The insoluble mineral matter was found to con-
sist of " :—

•Annual Report, Ueol. Sur\. Can., vol. VII. (N.S.), 18',I4. p. 81 it.

BARLOW.

ECONOMIC GEOLOGY.

157 I

\ ' 'i\

.Silica fi • 24 per cent.

Aluiiiuia and ferric oxide lal it

Lime OS!)

M: ■rnesiii 008

Alkalies (•;) 050

Total

S(;-2

Marl is often used as a fertilizer, and deposits such .is that exposed
at Emerald Lake should be of value locally for this purpo.se.

Grindstones and Whetstones.

Some of the matei'ial contained in portions of the beds of coarse Grim; itones.
sandstone and grit, found near the base of several of the Palu'ozoic out-
liers, would probably be suitable for the purpose of making grindstones.
A quarry was opened many years ago on one of these arenaceous
beds exposed above Deux Kivieres which furnished some excellent
grindstones. Where the layers are not thick enough for this purpose,
they would fuinish whetstones of very fair (juality. Where too hard
and compact, these stones answer only for a short time, when first
used, soon becoming too nmch polished.

Portions of the very fine-grained, banded slates and greywackes so
frequently met with throughout the northern and north-eastern part
of the district may probably allbrd material suitable for hones and
whetstones.

Clay for Bricks and Earthenware.

Cliiy suitable for the manufacture of bricks, extends over a very Clay,
large area in the northern part of Lake Temiscaming, from the vicinity
of the combined mouths of the !Montre.al and ]\Iatabitchouan rivers,
northwards far beyond the conlines of the present map. The bricks
for the large convent and church built V)v the missionaries of the Oblat
order at Bale des Peres were made there. In the vicinity of North
Bay, and extending thence some distanrie bej'ond Verne, brick
clay is readily accessible, although sometimes concealed by the presence
at the surface of varying thickness of yellow sand. A brickyard was
in successful operation at North Bay for some years, and if the local
demand were sufficient it would no doubt be re-opened. Some of these
beds of clay might also furnish material applicable for the manufacture
of coarse earthenware, but so far no clays fit for the finer kinds of
pottery have been found in this region.

Mica.

Both biotite and muscovite are among the con)monest constituents Mica,
of the various Laurentian gneissic rocks, but although thus widely dis-

I : 'r

158 I

NIPIS8INO AND TEMISOAMIXO REGION.

tributed their presence in this association is not of economic import-
ance. The numerous and often large pegmatite d^'kes tliat cut these
Laurentian rocks give promise, in places, of affording a supply of mica
in sheets sufliciently large and in such quantities as to be available for
economic purposes. The southern portion of the Township of Calvin
is peihaps the most important of these localities, but so fai- the musco-
vite obtained, represenling the material exposed at or near the surface,
has been too inferior in quality to command a price commensurate
■with the cost of mining. The opening up, however, of a large portion
of the south-eastern portion of the area of the Lake Nipissing sheet for
settlement, may bring to light other masses of {)egmatite producing

good mica.

AsJ>ei-(ufi.

Asbestus. This mineral has been found in the district. One of these localities

is situated near the west shore of the " Mattawjipika" on Lady Evelyn
Lake, on the Haycock mining location. It is also known to occur to
the north-east of Baie des Peres, but the deposits thus far discovered
are not very extensive.

G'i-aphite.

Graphite. This mineral, .so abundant in the Laurentian area further to the

south-east, is of rather rare occurrence in the region under descriptions
and although doubtless present as an occasional constituent of some of
the gneissic rocks, its {)reseuce was only noticed at one locality, where
it occurs disseminated in minute grains and scales throughout the
biotite cyaiiite-gneiss exposed near the shores of the Ottawa in the
vicinity of Les Erables llapids and Snake Creek. Its presence in a
rock-niMSS has oft-n been referred to as evidence of its sedimentary
origin, but in this instance there seems to be no doubt whatever
that the rock containing it ia a rather unusual phase of the biotite-
gneiss, and as such is to be considered as a foliated plu tonic mass.

Apatite.

Apatite. This mineral, though abundant as an accessory or accidental con-

stituent of many of the crystalline rocks occurring in this region, has
not yet been found in deposits possessing any commercial value.
The only locality where it was noticed in such quantity as to be
recognizable without the aid of the microscope, is on the property of Mr.
Emery llacicot, on lot 4, con. VI., of the township of Ferris, a short
distance from Nosbonsing, a tlag station on the Canadian Pacific Rail-

BARLOW

•J

ECONOMIC GEOLOGY,

159

way. A pegmatite dyke is here exposed, composed chiefly of very pure
and coarsely cleavnble llesh-red orLhoclase, with which is associated a
much smaller ([uantity of black biotite often in large cleavable frag-
ments. The dyke is about six feet in width, has a direction a little
west of north, according with the foliation of tlie garnctifcrous horn-
blende-gneiss with which it is associated. The apatite occur.5 very
sparingly, generally in small well developed prismatic crystals imbed-
ded chiefly in the biotite. Some of the crystals noticed presented the
following comVjination of faces : oc P. P. OP. oo P2. Most of the
crystals were too fragile, on account of their long exposure, to admit of
their being liberated without breaking from the material in which they
were inclosed. The felspar in this and other dykes in the near vicinity
is very pure, and large pieces, many pounds in weight, could be readily
secured without any admixture of foreign matter.

Fl'uorite.

Fluorite or fluor-spar is found in large cleavable masses, associated Fhiorite.
with orthoclase, niicroclino and perthite in the large pegmatite dykes
that cut the biotite-gneisses in the township of Cameron, about four
miles and a half east, of Mattawa. The fluorite is of a light-greenish
colour, but like the felspathic constituents of these dykes, is very much
stained and infiltrated with ferric hydrate, which fills the numerous
cracks and fissures present in the mineral.

Molybdenite.

The presence of this mineral, as an occasional constituent of quartz Molybdenite,
veins, has been noticed in the district immediately surrounding Lake
Nipissing. It is stated to occur in considerable quantity to the north
of Talon Creek, on the Mattawa River, although its presence there
was not verified during the progress of the examination of the region.

Steatite,

This mineral, usually a decomposition product of basic pyroxenic or Steatite.
hornblendic rocks, is not very commonly met with, but specimens were
obtained of tolerably pure material from the west shore of Luke Tem-
iscaming, about four miles south of the Montreal River.

Amazon-stone and Perthite.

These two minerals are intimately associated with one another, con- Oiiiaumntal
stituting much of the felspathic constituents of some pegmatites which stones.

i I

160 I

NIPISSING AND TEMISCAMING REGION.

Openings
made.

cut a readily disintegrating biotite-gneiss, that outcrops on lot 7, con.
B, of the township of Cameron, about four miles and a half east of
Mattawa. Four openings have been made, of the nature of small
pits or shallow trenches, extending only a few feet below the surface.
The largest dyke is about five feet in greatest width, running north-
east and south-west. The railway line is about 200 yards to the north,
while the Ottawa River passes about 500 yards to the south of the
exposure. The openings were made for apatite, and work on the pro-
perty was abandoned when this material was not found. The aniazon-
stone, when fresh, is of a very beautiful deep bluish-green colour,
but owing to its proximity to the surface much of the material is more
or less stained, and the minute crevices are filled with ochre. This
defect would doubtless soon disappear in depth. Some of the material
secured at the insignificant depth reached by the present workings is
remarkably good, and is suitable for cutting and polishing.

The perthite which is intimately associated with the amazonstone
at this localit)', is a pale flesh-red aventurine felspar, shown to consist
of a fine interlamiaation or parallel intergrowth of albite and orthoclase.
The alternation of the darker-coloured flesh-red orthoclase with the
paler albite, and the accompanying brilliant aventurine reflections pro-
duces a beautiful stune when cut and polished.

Cyanite.

The occurrence of this mineral in situ in Canada was first noticed
by the writer in 1890, in a cutting on the main line of the Canadian
Pacific Railway, about half a mile east of Wahnapita; station. Here
Cyanito. it occurs in flattened blade-like crystals and fragments, in association

with a reddish alniiindine garnet in a mica-diorite-gneiss. The
crystals usually conform to the foliation, but sometimes they occur in
groups and clusters disposed at varying angles to the schistosity. In
the more basic portions of the gneiss, the crystals are darker in colour,
and have undergone in places ratlier extensive cracking and deforma-
tion as a result of pressure. In the more acid or pegmatitic portions of
the rock, the cyanite is much lighter in colour and occurs in stouter
prisms. Fibrolite (siilimanite) also occurs in this locality, developed
chiefly along certain crevices in the gneiss. It is fibrous or finely
columnar in structure, and is traversed at right angles to the fibres by
numerous fine cracks. Sometimes it occurs in curious irregularly
radiating or plumose aggregates. The colour when fresh is of a pale
bluish-gray.

ECONOMIC GEOLOGY.

161 I

During the examination of the Ottawa River above Mattawa,
cyanite was again noticed as a constituent of the biotite-gneiss
exposed in the cuttings on the Temiscaming branch of the Canadian
Pacific Railway in the vicinity of Les Erables Rapids and Snake Creek.
Here also it occurs in long, thin-bladed crystals in association with
red garnet, and is in many places so abundant a constituent of
the gneiss as to characterize this rock. The crystals are usually light-
bluish or greenish, but some show a beautiful deep azure-blue centre

with white margins.

Fossil Corals.

The particularly fine fossil corals of the Niagara outlier exposed on Fossil corals,
the shores and islands of the northern portion of Lake Temiscaming,
which have undergone in most cases complete silicification, would
doubtless not only command a ready, though somewhat limited sale
as specimens, but when polished would form an attractive ornamental
stone for certain purposes. The west side of Mann Island exhibits
abundant specimens of this kind.

Springs.

The region, as a whole, is not characterized by abundant springs, Springs,
although occasionally some large ones are encountered. Opimika
Creek, reaching Lake Temiscaming from the west immediately north of
the narrows of the same name, is chiefly fed by springs, as is also
Latour Creek, which enters the same lake on the west side about four
miles above the Old Fort Narrows. Both these streams are remark-
able for the coldness and clearness of their waters, and for the fine
specimens of brook trout to be found in them. A fine large spring
rushes down the hill immediately behind Thompson Bay, below the
Opimika Narrows, on the east side of Lake Temiscaming, about half a
mile east of the old Hudson's Bay Co.'s post. Another spring of good
water flows down at the head of Les Erables Rapids on the
Ottawa. As the country becomes settled many new springs will be
found, but the abundance of good water contained in the many lakes
and streams of the region, renders the presence of springs much less
important, although as a rule the water in these lakes is rather warm
for drinking purposes during the summer months. During a consider-
able portion of the summer, the presence of a large number of minute
greenish or yellowish particles, often so abundant as to form a scum at
the surface or around the margins of the lakes, renders the water of
many of them more or less unfit for drinking purposes. The waters
11

' ,ii

' .! ':

i}i.:

1(J2 I

NIPISSING AND TKMISCAMINO REGION.

of the springs that feed Emerald Lake, at the head of one of the
branches of Opimika Creek, have ah-eady been referred to. They are
the only ones known to possess therapeutic qualities.

Lfiiptli cif
river included.

Its course .ind
lakes uii it.

RE(aONAL DESCRIPTION.

The Ottawa River and Lake Temiscaming.

General Features.

As may bo seen by a reference to the accompanying map-sheets, a
considerable length of the Ottawa is included by them. From the
north-east bay of Lac des Quinze, where it enters the Lake Temisca-
ming sheet, to the mouth of the jNIattawa (which for convenience has
been included in the southern sheet) the distance is about 142 miles.
Three large Jakes occur in this distance, which may be regarded simply
as expansions of the stream.

The most northern of these expansions, known as Lac des Quinze, is
very irregular in outline, with several long arms or Ijays running in
various directions, but the most direct line of comTuunication through
the lake measures about twenty-two miles. This lake is separated
from Lake Temiscaming by a short stretch of water known locally as
the " Quinze River," noted for its wild and dangerous rapids, and
which in its eighteen miles of length falls a distance of two hundred
and sixtj' feet. Lake Temiscaming, into which this stream empties,
is sixty-seven miles long from the mouth of the Quinze to the head of
the Long Sault Rapids, while Seven-league Lake, which commences at
the foot of these rapids, adds a further length of seventeen miles.
While it would thus appear that the river, strictly speaking, embraces
only about thirty-eight miles of this whole distance, it may be stated
that a considerable proportion of that generally included as lake should
in reality be considered as portions of the river proper. A large part
of these water-stretches exceeds but very little, if at all, the average
width assumed by the river when not obstructed by rapids, while at
several points a swift current is present, denoting a small though
appreciable change of level.

Thus Seven-league Lake, in its lower portion, is only about a
lake stretches, quarter of a mile wide, while in the upper part it never exceeds half
a mile. In this lake a light current can usually be detected, showing
a total fall in the whole length of about a foot during the ordinary low
water of summer ; but during times of freshet this current is aug-
mented, and the total fall is increased to a little over two feet.

River-like

■]

Tin: OTTAWA A\D LAKK TRMISOAMIXr,.

163 I

Lake Tomiscaming itself, as noted in the appendix, shows a differ-
ence in level of ii ioot from the head of the Long Sault llapids to tlie
wide portion above tlie Old Fort Narrows, while the lower portion of
the lake south of the mouth of the Montreal River, is quite river-like.
This diiference in level is maintained by three \evy pronounced con-
tractions. The most northerly of these is at the Old Fort Xari-ows,
where the lake is pinched in between two bold hills of gravel, leaving
a channel a little less than 800 feet wide at oi'dinary stages
of the water. At the Opiinika Narrows, about thirty-tive miles
further, a .still more pronounced current Hows through a strait which
at one place is less than 200 yards in width. This current,
formerly kno'vn tc the old voyageursas "La (^abre " shows a descent
of fully half a foot. At Presquile, about a mile north of the head of
the Long 8ault, the third contraction occurs, and here again a consider-
able current may be noticed, but not so strong as at the Opimika.

The Ottawa, from the north-east bay of Lake des Quinze, has a general ( Joneral direc
direction a few degrees south of west as far as the head of Lake Temis- '"" " "^''-'''
earning. At this point, however, it suddenly changes, and from the
head of this lake, as- far as the luouth of the INIattawa River, the sti'eam
flows about S. 30° E. In places there is a decided divergence from
this general course, caused by local bends, which are especially char-
acteristic of the upper portion of the ri^■er, but from Lake Temiscaming
to the jNIattawa, the river follows an unusually uniform and deep
valley, and any bends which do occur are in the nature of large curves.

The upper part of the river, above Lake Temiscaming, occupies a ch.aracter of
very pronounced valley, and the hills around Lac des Quinze present ^""■H'^y'
the usual rounded or dome-like outlines so distinctive of areas under-
lain by the Archa\an gneissic rocks. Except on the northern
portion of the lake, where they are unusually bold, ranging from
200 to 300 feet in height, the hills are as a rule low, averaging
less than 100 feet. The Quinze River, which usually breaks
across the strike of the inclosing rocks, occupies an original,
but not very pronounced depi'ession. When Temiscaming is reached
these conditions undergo a decided change ; and the valley, especially
in the lower portion, is fiord-like in aspect. From the Mountain
Rapid to the mouth of the Mattawa, the river brejiks across irregular
ranges of hills, which rise very abruptly from the water to heights of
from 400 to 600 feet, while the shores on either side of Seven League
Lake, which are as a rule bold and rocky, preserve a rather constant
elevation of from 200 to 300 feet. In the construction of the Lake
Temiscaming branch of the Canadian Pacific Railway along the rocky

I'r

! i

illhi

,1 ,

:hi. 1

> ,i '

164 I

NIPISSING AND TEMISCAMING REOIOX.

Illlf

Montreal
Kivcr to
Lons Sault.

West shore.

eastern bank, this was so steep and abrupt that it was found necessary
in most instances to make large rock-cuts, the road skirting the shore.

From the mouth of the Montreal River to the Long Sault Rapids,
the banks on both sides of Lake Temiscaniing are extremely bold, and,
as a rule, rocky, and frequently for several miles present unbroken
cliflfs. The hills on both the Ontario and Quel)ec sides of the lake rise
very steeoply from 3-")0 to GOO feet, with but few minor and unimport-
ant breaks where some of the larger streams flow in. Throughout the
whole of the distance from Mattawa, the tributary streams all show a
very abrupt descent tf) this valley. Above the mouth of the ^Montreal,
the topographical outline changes somewhat suddenly, and the shore,
though still in many places steep and abrupt, is not continuously so ;
while wide and open valleys covered with drift separate the still high
hills. The west shore of the lake is especially steep and regular, and
until Haileybury is reached no ilat of any appreciable extent occurs.
Near the north-west corner of the lake, large and comparatively level
tracts exist that extend far beyond the boundaries of the accompany-
ing map, and are fast being opened up for settlement.

East shore. The eastern, or Quebec shore, presents many deep and important

indentations and although numerous high and exceedingly rugged
hills occur, they are for the most part separated from one another by
flats of clay. These have in many instances been cleared and are at
present occupied by prosperous farmers, the soil being good and yield-
ing abundant crops.

Head of Lake The depression occupied by Lake Temiscaming extends in a north-

8 aming. ^gg^gpjy direction, but becomes divided into two subsidiary valleys by

the flat limestone promontory terminating in Dawson or Waljis Points.

These valleys are occupied by the two important tributaries known as

Wabis Creek and the Blanche or White River.

Soundinps by
T. thierin.

It has always been known that the Ottawa River is, in many
portions of its course, very deep, but no accurate information regarding
its depth was published until Mr. Thos. Guerin, C. E., examined that
part of the river above Mattawa.* Those soundings were, however,
few in number and confined chiefly to Seven League Lake, although a
few were obtained in the vicinity of Chiefs Island on Lake Temisca-
ming. Mr. Guerin states that Seven League Lake was sounded in
several places, the depth obtained being generally about sixty feet. In
one place it was 397 feet, but in no place was it found to be less than
thirty feet deep. The sounding-line on Lake Temiscaming was unfor-

*Annual Reiiort, Minister of Public Works, 1884-85, pp. 106-107.

■MLOW.

tunatelj
Chiefs

Durii
nights V
were coi
was foui
liere stei
bouldeis
greatest

Fou.
showing
bottom.
About m
channel
shore is (
considera
of which
the culm

From <
soundings
feet and 1
211 feet
200 yards
again appi
centre was
it shallows
shallow po
which Mel

All of tl
gravel or s
rapidly anc
Keepawa 1
noted was
mid-stream
tained clos(
of the west
from the e«
lake is 423
Rock it is 4
little over s
lake, the de

A!;iAi.-

■]

THE OTTAWA AM) LAKK TEMISCAMING.

1G5 I

tunately only 120 feet long, and on continuing the soundings south of
Chiefs Island it soon failed to reach the bottom.

During the progress of the (Jeological Sui-vey several calm moonlight Soundinprs hy
nights were spent in sounding Lake Icmiscaming. iliese soumungs Smvty.
were commenced at the Opimika Narrows, where the deepest water
was found to occur in close proximity to the westei'n shore which is
here steep and rocky. The bottom is composed of coarse gravel and
boulders, and the lead showed a narrow and tortuous channel whose
greatest depth was forty-five feet •

Four more soundings were taken in going north, in the next mile, Opimika
showing a gradual deepening with a gravelly and ultimately a sandy M'L•^lal■till
bottom. These soundings were respectively 55, 47, 75 and 111 feet. l'"'i't.
About midway between Main Channel Islet and the west shore, the
channel is 65 feet deep, while that between this island and the eastern
shore is only 55 feet. It is evident that there exists at this point a
consideral'e bar, due to the deposition of inorainic or drift material,
of which Main Channel Islet (wholly composed of boulders) forms
the culminating point.

From this place to within half a mile of McMartin Point, three
soundings were taken, showing an increase first to 95 feet, then 139
feet and 183 feet, while three soundings taken at this point showed
211 feet in mid-channel, and 198 and 127 feet, the latter being within
200 yards of the western shore. Opposite McMartin Point, the lake
again appears to shallow somewhat, and the deepest sounding near the
centre was 157 ^'f-et, while half way between this and the western shore
it shallows still further to 130 feet. Again it would seem that this
shallow portion is caused by an accumulation of morainic debris, of
which McMartin Point forms the shoreward extension.

All of the above soundings showed a bottom composed of very fine ^McMartin

gravel or sand. To the north of McMartin Point, the lake deepens J*"'"t to

, , . , Keopawa.

rapidly and maintains a very uniform depth as far as the mouth of the

Keepawa River. About a mile north of McMartin Point, the depth
noted was 425 feet, while still further north, opposite Latours mills, in
mid-stream, the depth found was 460 feet. This great depth was main-
tained close to either shore, for a sounding taken within ten chains
of the western shore showed 455 feet while one taken an equal distance
from the eastern shore was 320 feet. About a mile further north, the
lake is 423 feet deep and again in mid-channel opposite the Buffalo
Rock it is 430 feet deep. The deepest sounding made was taken a
little over a mile south of the Keepawa River, about the middle of the
lake, the depth being 470 feet. Going northward, the lake shallows,

r-{ ■■

16G I

NIPISSING AND TKMISCAMINfi KKGION.

Ko('pawa to

Montroal

Uivor.

Montreal
River to
Old Fort
Narrows.

Morainio

deposits at
Narrows.

and oj)posite the mouth of the Keepawa is only 362 feet deep. Through-
out this interval of great depth, from IMcMartin Point northward, the
whole bottom was found to be covered by a soft, unctuous, gray clay
or ooze into which the lead sank a foot or more.

The depth ascertained at the mouth of tlie Keepawa remains uni-
form to within a mile of the combined mouths of the Montreal and
INIatabitchouan rivers, where it is 317 feet. Northward, the lake
gradually shallows, and opposite the mouths of these streams has
been partly filled up by an extensive deposit of sand and gravel
that forms the bottom in this neighbourhood. These streams cannot,
however, account for the vast accumulation of loose material which is
here evidently jiresent, for the lake is over a mile wide, and for more
than a mile in length has been filled up by a deposit varying from 100
to 150 feet in depth. Further, the lake shallows considerably to the
north of these streams, while the reverse would have been the case if
the whole of the material had been brought down by them. This
extensive bar has probably been deposited in the first place as a lateral
moraine, in the shelter of the bay in the rocky hills that occur at the
mouths of these rivers, while the material subsequently transported
and laid down by the streams, has reformed and modified these depo-
sits, producing the somewhat wide delta now found.

Opposite the mouth of the Montreal Ptiver, the depth of the lake in
the middle is 275 feet, while about three-quarters of a mile further
north this again decreased to 2.")6 feet. Still further north, the lake
deepens rapidly, and two miles north of the ^Montreal River the sound-
ings showed a somewhat uniform depth of 400 feet. A little over
half a mile south-east of Roche McLean, the lake is 378 feet deep,
while opposite the north end of Quinn Point it is 370 feet. Here
again a bar composed of boulders and clay with a little sand extends
from the north-east end of this point for nearly a quarter of a mile,
with only about five feet of water at ordinary summer level. In the
centre of the large open space to the north of Quinn Point, the lake
is 348 feet deep, while in the middle of the Narrows, opposite Pointe
a la Barbe, it is only 170 feet deep. In the open space opposite the
mouth of the Little River it is !'< 5 feet deep, thus showing a rather
uniform depth in this portion.

The Old Fort Narrows is a very decided contraction occasioned by
two bold hills of sand, gravel and boulders. The deposition of the
material at this point was evidently determined by a pre-existing rocky
narrows, the higher portions of which may be seen protruding from the
surrounding mantle of sand and gravel. During the retirement of the

•]

THE OTTAWA AXD I.AKK TEMISCAMINfJ.

ir,7 I

ice-shect up the valley of the luko, a large amount of moniinic material
was deposited at this place, thus still further reducing the channel.
In the oliannol, immediately opposite the Hudson's l>ay Co.'s old store,
the first sounding showed a depth of 31 feet, which was gradually in-
creased to about sevonty-ti\ e yards from the west shore ; while less
than thirtj' yards from the west shore tlie depth was found to he 46
feet. To the north, the lake gradually deepens, first to 88 feet about
an eighth of a mile north of the Narrows, and finally to 120 t'eot about
half a mile north. In the opposite direction, or southwards, on the
other hand, the lake deepened first to C.J and then to 1.30 feet within
less than an eighth of a mile.

There seems, therefore, to be no warrant for the supposition that
this barrier of sand, gravel and boulders p-:tended at one time com-
pletely across the lake, for, if such had been the case, it appears probable
that the removal of this material would have resulted in the accumula-
tion of a considerable deposit immediately south of the Narrows, which
is not found, as the descent on the south side is nmcli steeper, in
fact nearly as steep as the angle of repose, under the conditions, for
gravel and sand.

Our soundings did not extend further to the north, and 'ilthough x^ gomjjii„„g
the western shore-line is still very steep and abrupt, it is not probablt; '" "ortliorn
that tlie great depth characteristic of those areas to the south of the
Narrows is maintained in this direction, although occasional localities
with considerable depth may doubtless be found, presumably in the
neii'hbourhood of the western shore.

The highest water in this part of the Ottawa is in general occasioned Times of
by the melting of the snow in spring, and occurs usually about the "^S^' ^"'' '"^'''
latter part of May, while the time of low-water is during kSeptember or
October, according to the setting in of the autumn rains. During the
summer months, the Ottawa is remarkably and quickly affected by very
heavy or long continued rainfalls. In ordinary seasons this ditierence
in level varies from twelve to fourteen feet, but in 1887, and again in
1894, Lake Temiscaming and this portion of the Ottawa showed the
astonishing difference of twenty-one feet between the two extremes of
high- and low-water. Both of these years were, moreover, remarkable
for an extremely heavy snowfall during the preceding winter, thus
furnishing conditions for an extraordinary spring freshet, while the
succeeding summers were notable for excessive and long continued
drought, and the lowest water occurred during the month of
September.

- i

iiiji'

!ii

^^[.-■i

iii'i

168 I

NIPI.SSINO AND TEMISCAMINO lUXlION.

Differnncp in

full I if lion^'
Hivult KapulH

One of the most marked oll'ects occasioned by this difference in Inv el,
is the corresponding difl'erence in the fall of the Lont,' Hault llapids
that separate Lake Teniiscaminj,' from Seven League Lake, and the
accompanying increase in the fall of the rapid at \\w outlet of the
latter, known as " The Mountain.' During times of low-water the
fall in the Long Sault Rapids is almost lifty-livo feet, wliilc at high-
water it is only forty-nine feet. On the other hand, during tinvs of
freshet, the Mountain Rapid has a fall of seven feet, while at low-
water there is only a fall of a little over three feet. During the same
time Seven League Lake has a total fall of two and a-half feet in times
of high-water, and at low-water there is only a fall of half a foot from
the noith to the south end. These seeming anomalies are thus
Exiilanatic'ii explained by Mr. Thomas Guerin :* — •" The Long Sault * * * is
y. 1. nim . jj^j^ig,] jj^ j^g head by an island into two channels, tlie level of the
bottom of the eastern channel being about seven feet below that of the
bottom of the western channel which becomes dry at low-water.
* * * The outlet from Seven League Lake is at the ^Mountain
Rapid, and the capacity of the channel here is less than the united
capacities of the two channels, which constitute the outlet from Lake
Temiscaming. Hence the latter channels during high-water pour a
greater (juantity into Seven League Lake than the outlet of the latter is
able to dischai'ge, thus causing Seven League Lake to rise, while Lake
Temiscaming falls so that the difference of level nmst be least at
high-water. Again when the level of Lake Temiscaming falls so low
as to render the western channel dry then the outlet from Lake Tem-
iscaming will be confined to the eastern channel, which is nearly of the
same dimensions as the outlet of Seven League Lake, but as the area
of the latter lake is many times less than that of Lake Temiscaming,
its level must fall faster and the difference of level must be greater
at low-water than at any other time."

Discharge.

Trend of
Ottawa

Valley.

The rate of discharge from Seven League Lake was measured by
Mr. Guerin at the current immediately above the Mountain Rapid, on
. the 21st of August, 1884, and found to be 16,383 cubic feet per sec-
ond. From a comparison of the levels then prevailing, it was calcu-
lated that the rate of discharge during times of high-water would be
25,100 cubic feet per second, and during low water 14,800 cubic feet
per second.

The trend of the Ottawa Valley, from its confluence with the
Mattawa to the foot of Lake Temiscaming, is nearly north-west, mak-
ing a considerable angle with the direction of the foliation of the

* Annual Report, Minister of Public Works, 1884-85, pp. 107-108.

•ANLOW

THE OTTAWA AND LAKK I KMlSCAMINfi.

1G9 I

gneissic rocks ulong its hfinks. At the mouth of tho Miittawa a .sharp
elbow is formed, the valley below that river turuiiij,' nearly cast, in
close correspondenoo with the foliation of the gneisses and coinciding
in direction with tho depression occupied by the ]\[attav\a Hiver. The
sharpness of this elbow is further accentuated l>y the fact that, for
several miles above this point, tho course of the Ottawa River is nearly
north-and-south.

The river from IMattawa to the foot of Lake Teniiscaming is inter- ijaimls,
riipted at intervals by hea\y rapids, three of which occur f)n the lirst i,,|i<,.''|','.t„i8.
fourteen miles, while the Long Sault, seventeen miles further up, is «-!'ii""g.
six miles in length.

The first rapid, four miles above the Mattawa, is now known as La j,,, Cave.
Cave. It is about half a mile in length, and is divided into two leaps,
the lower of which was formerly known as La Cave, while the upper
portion was called the Demicharge Chaudron, or Chaudicre. The
The combined fall is nearly ten feet, divided into two nearly equal
parts. The river between the Mattawa and La Cave llapitls a\erages
about a quarter of a mile in width, although in one or two places where
bays are present, this width is nearly doubled. Antoine Creek is the
main tributary in this interval, coming in from the west and draining
in its course the larger portions of the townships of Mattawa and
Olrig, its source being in some small lakes situated in the south-western
part of the township of Erench.

From La Cave to the next rapid, known as Les Erables, is a little Les Erables.
over three and a half miles, while the width averages about a third of
a mile, aud occasionally somewhat less. Les Erables Rapids are a
little over half a mile in length, with a descent of nearly thirteen feet.
Latour Island, at the foot of this rapid, and almost in the middle of the
current, shows a large number of pot-holes worn out in the rock. All
stages in the process may be seen from the incipient canals, where the
eddies have commenced to wear down along the jointing planes that
cut the rock, to holes ten feet in diameter. In a few instances several
holes are seen to liave been so greatly hollowed out that they ultimately
joined at or below the surface.

Cotton Creek enters from the east a short distance below the foot of
Les Erables Rapids, forming a beautiful cascade as the water tumbles
over the rough ridges of gneiss which impedes its progress. This
stream drains a number of lakes, of which Lake Memewin, situated
about four miles to the east of the river, is the largest, being four
miles long, and very irregular in outline. Scarcely three miles and a
half intervenes between Les Erables and The Mountain, where the

I !

170 I

NIPISSING AND TEMISCAMIN(i REGION.

Tlic Arouiitain wliole volume of the river flows throuah n narrow ch.annel, obstructed
by rocky reefs and islets. About a mile above Les Erables Rapids
anotlier stream enters from the east, with a steep descent into the

Snakf Crook, valley of the Ottawa. This stream, now known as Snake Creek, drains
a nuinV)er of small lakes, the largest of which is Snake Lake, while the
head waters are in a small lake, from M'hich only a short portage is
necessary to reach Obasking Lake. It thus formed a portion of the
old winter route, which left the Ottawa River at the mouth of this
creek and reached Lake Temiscaming a short distance below the
Opimika Narrows. About a mile below the Mountain Rapid one of
tlie highest hills was ascended and found by aneroid barometer to be
520 feet above the surface of the water. The average height of the
hills on either sitle would, therefore, be little less than 500 feet.

Seven Loa{,'uo
Lake.

Streams
entering
East Crook.

Jocko River.

Its southern
branch.

Seven League Take, is a stretch of navigable water nearly seventeen
miles in length, extending from the head of the ^lountain to the foot
of the Long Sault Rapids. The banks in most jjlaces are steep and
rocky, and one or two places, perhaps, deserve special mention. Devils
Garden Bluff, on the east sid presents a sheer precipice of gneissic
rocks, and receives its name from the fact that a patch of wild onion
grows near its summit. Above this, on the west .side and only a short
distance below the foot of the Long Sault Rapids, there is a sharply
accented hill thickly overgrown with small pine trees, which, from its
niaiked resemblance to the characteristic headgear of the Canadian
"habitant," has always received the designation of "La Tuque." This
is a rather important and well known land-mark.

Three important tril)utaries enter Seven League Lake. The first of
these, known as East Creek, has its source near the eastern limit of
the southern map-sheet, and is thus not more than seven miles long,
reaching about six and a half miles below the foot of the Long Sault.
The next stream, however, which enters on the west side about half a
mile further north, is much larger, and named Jocko River, after a
half-breed of that name. Formerly the stream was known as the
Siconaguisipi or Blackstone River, a name appearing in Sir William
Logan's report on the region, although on his manuscript map it is
designated as the Porcupine River. The main branch of this stream
heads in a lake about two and a half miles long, bearing the same name,
and situated about the centre of the township of Osborne, a little over
twenty p^iles in a straight line from the outlet. Its northern blanches
drain the northern parts of Osborne and Garrow townships, and also
a considerable area of unsurveyed land between these townships and
Nevins base-line. The southern branches drain almost the whole of

■1

THK OTTAWA AND LAKK I'UMISCAMINC!.

171 I

the townships of Stewart an<l Lockhart, this area being but sliglitly
less than stivcnty sf|uare miles. The river has carried down a quantity
of loose material, which fills up a large area of the lake in the vicinily
of its mouth. It Hows through a steep, narrow valley, and in debouch-
ing on the lake the channel makes a sharp bend northward through
the gravel and sand, ilius forming what has often been called a " square
fork." This delta is 200 yards wide and about a quarter of a mile long,
and may owe its origin partly to glacial accumulation and deposition.
If it occurs as a result of stream action, it evidences a river of much
greater volume than that which now occupies this valley.

TheObashing is the third stream of importance entering Seven ^ j. ague Ohashinc:
Lake in a bay on the east side, close to the foot of the Long Sault
Rapids. The lower portion of this stream meanders through a sandy
Hat, which extends inland for some distance. The upper portion of the
stream, however, is exceedingl}' rough and rapid, showing a total fall of
about 300 feet in a distance of scarcely three miles. It attbrds an
outlet to a large number of lakes in the region to the south of Keepawa
Lake, the largest of which is Obashing Lake. The name is of Chippewa
origin, and refers to the narrows which divide the lake into two very
nearly equal portions. It covers an area of about eleven square miles,
and measures ten miles from east to west, with an average witlth of
from one to three miles. Two laige tiibutaries enter the eastern end
of the lake, the most northerly being known as the Otter River.

The Long Sault Rapids separate Seven League Lake from Lake 'I'hc Lonp f
Temiscaming, and are caused by a great accumulation of very coarse ' ''" ^"■^"' ^
gravel and boulders, many of the boulders, at the head of the rapids,
are exceedingly large, measuring from twelv^ to fifteen feet in diameter.
Tlie rapids are usually very narrow ai,w ore ked, and a little over six
miles in length. Very little rock in, s".''t • .-'n now be seen, although it
is evident from the topography tL.\t the detritus was deposited in a
pie-existing shallow narrows. On the east, or Quebec side, the drift
material forms a comparatively level space, varying from a quarter tc
half a mile in width, along which the railway-line is constructed. With
skilful canoemen, it is customary to run the Long Sault Rapids in the
larger voyaging canoes, but five portages and tracking lines are neces-
sary when an ascent is made. The three lower portages are on the
east side of the stream, and the two upper ones on the opposite bank.

Two streams fall into the Ottawa at the Long Sault, one from either McDouKall
side. McDougall Creek, which flows in from the west at the '\"'' '•"'"''''"
Crooked Rapid, takes its rise in some small lakes about ten miles to
the north-west, and Gordon Creek enters about a mile below the head

r !■

172 I

NIPISSIXG AND TEMISCAMING REGIOJf.

Lower I'lul II
JiiiUc TeliiiH-
caiiiing.

Lengtli :iiii
area.

Forest
growth.

!Moraiiiic
islands.

Opiinika
Narrows.

of the Lom;,' Saiilt. Logs are bnjught f'ruiii Ivecpawa Lake by an
artificial cliannel into Gordon Crepk, down which they are run. The
total fall of (Jordon Creek, fi-oin Keopawa Lalco, is about 300 feet,
nearly 250 feet of which is below Pike Lake in a little over a mile,
f Lake Teniiscaming is usually regarded as coiuuiencing at the head
of the Long iSault. The name means literally "at the place of the
deep dry water," doubtless referring to the existence of the extensive
clay flats in the north-eastein jiortions of the lake which are soiuetimes
dry. ll;e lake is sixty-one miles long in a bi>aring N. 2G' W., with
an area of about 125 S(]uare miles. From the head of the Long Sault to
the Narrows the lake is about a quarter of a mile wide, but at the foot
of the Narrows it increases in width to about a mile, on account of
Thompson Bay, situated on the east side. Both shores are steep
and high, and in several places there are almost perpendicular clifls
over 200 feet in height. On the Ontario side especially, the hills are
covered with a good growth of pine, almost to the water's edge, which
eftectually conceals the rock l)eneath. A portion of the Quebec side,
between the Narrows and Schooner Island, has, however, been almest
denuded by fire of its ori^anal forest growth, and exposes the rough
and broken ridges of gneiss, SchoDner or Ship Island evidently
represents the apex of a bouldery shoal, as no evidence of a rock in
situ could be found. Presquile, about a mile above the head of
the Long Sault, has been designated as an island, and although com-
paratively deep bays approach close to one another on the north and
south sides, a small neck of land unites the so-called island with the
eastern shore. It evidently I'epresents an older accumulation of
morainic material which in so many places block the channel of the
river.

The Opimika Narrows, are about two miles in length, and very
crooked and contracted towards the northern end. High rocky
hills form the immediate coast-line on tlie west side, but on the east
side the shore is composed of sand, gravel and boulders, forming a flat
over a quarter of a mile wide to the base of the rocky hills. The
greatest conti-action is towards the north end, where the shore-lines are
only a little over a hundred yards apart. Two creeks enter the
Ottawa at the Opimika Narrows. The largest one, now known as
White Creek, drains two or three small lakes between this point and
Keepawa Lake, the largest of which, White Lake, is over half a mile
in width, and two miles in length ; the eastern end approaching within
about three miles of Keepawa Lake. The other creek is known as
Green Creek, and enters from the west side, draining some small lakes
in that direction.

•]

THE OTTAWA AND LAKK TEMI^CAMING.

173 I

Above the Opimika Narrows the lake widens almost iiumediately, Narrows to
and from this point as far north as tlie mouth of tlie Monti eal i^iv"i.'^''
River it has an a"erage width of from three-quarters of a mile to
a mile. The shores are very bold, often exhibiting nearly vertical pre-
cipices of rock for many miles at a stretch. Occasionaliy small portions
of the shore-line are composed of sand and gravel, but high trees rise
almost immediately behind. MciMartin and Ouellette points are
small, low, projections running out a small distance into the lake
and are composed wholly of sand and gravel except in the case of Mc-
^lartin Point, where some of the solid rock projects through this loose
material. In the vicinity of Mc^lartin Point, a considerable amount
of stiff grey clay was noticed, and a bank of this contains a large nura-
])ov of very irregularly shaped calcareous nodules, but no fossil remains
were found in them. The hills on either side of the lake are from 300
to 500 feet above the surface of the water, and the highest, known as
the King of the Bea\( rs, rises to a height of about GOO feet. These
hills evidently form the edges of an undulating plateau which extends
inland on both sides, and in which the valley of the lake has been
excavated. P)uffalo Rock is another well known topographical feature,
consisting of •; r ,\y precipice on the west shore of the lake, and so
named from .., .iiass of vegetation upon it, which has a fancied resem-
blance in outline to a buffalo.

Six tributaries may be mentioned which (low into the Ottawa Trilintaries
between the Opimika Narrows and the mouth of the Matabitchouan ''"[''",'? ,""
River. The first of these is Opimika Creek that enters a beautiful
sandy bay on the west side, known as McLaren Bay, about half a mile Oi imil'iii
north of the Narrows. The water of Opimika Creek is extremely clear
and cold, abounding in speckled trout. Although its actual source is
in a small lake about nine miles to the south-west of the Narrows, it
derives most of its water from two lakes some four miles to the south-
west, which are supplied by a series of large springs. One of these
lakes is called Emerald Lake, and is remarkable for containing a deposit
of shell marl which is described in that portion of the report treating
of economic geology. The small pond at the head of the stream is 580
feet, by barometer, above Lake Temiscaming.

About thi-ee miles further on, Ottertail Creek reaches the lake from Ottcituil
the west. This stream forms a poi-tion of a route to the west. The
main or southern branch takes its rise in a small lake, some twenty miles
to the south-west in the township of J-lammell, within a mile of Spruce
Lake, at the head of the Tomiko River. About a mile above McMartin
Point, a small stream enters from the east, draining White Beaver Lake,

i I

I I

1 ,

! '!H

174 I

NIPISSING AND TlCMISCAMIXfl REGION.

Kc>('))awa
Kiwr.

SliniTs north
of .Montreal
Kiver.

and three miles south of the mouth of the Keepawa lliver, another small
stream enters whicli is notable as beitij,' the old Indian jiortage-route
to Lake Keepawa.

The next .stream is the Keepawa liiver, forming the outlet to a great
number of large lakes, many of which are outside the boundaries of f'.ie
present map. The largest of these lakes is of course Lake Keepawa,
which is nearly thirty-two miles in a straight line from north to south
and, with its intricate shore line of bays, covers an area of 120 square
miles. The Keepawa River is nearly nine miles in length, with a total
fall of about 300 feet, and has a number of powerful rapiils and
chutes in its circuitous course. At the mouth is a very fine chute.
The Matabitchouan and Montreal ri\'ers, which enter the lake at the
same place, are elsewhere separately described.

North of the [Montreal Kiver, Temiscaming Lake gradually widens.
The western coast-line continues to be ratluM- even aiid unbroken and
is also as a rule steep and rocky. At the Crows Nest liock, opposite;
Bryson Island, as well as at Manitou Jlock opposite Mann or Burnt
Island, there are sb.eer precipices, that extend for several miles vary-
ing from ir)0 to 200 feet in height. Tii.e east side of the lake shows
more irregularity in outline, and large areas of level land exist, from
which, however, bold hills rise in places. There is much more culti
vable land in the aggregate, than the often rocky character of the lake-
shore would indicate.

Islands.

Below the Old Fort Narrows there are only a few small and insig-
nificant islands. Roche McLean, so named after an old North-west
Company fur-trader, as well as the island north of Pointe a la Barbe,
are both connected at low-water with the western mainland by narrow
bars of sand and gravel. Moose Rock is a huge boulder of breccia-
conglomerate, about thirty feet in diameter, situated some four miles
south of the Narrows. North of the Narrows, there are several islands,
of which the mo.st important are Bryson or Moose Island, Burnt
Chiefs Island. Island and Chiefs Island, the latter being a well known topographical
feature. It is high and rocky, and at low-water is connected at its
eastern end with the mainland by a bar composed of boulders and
clay ; although, during the early part of the season, there is often
sutlicient water to permit of the passage of the steamer. To the north-
west of the island a similar bar exists, which, at low-water, prevents
the steamer proceeding any further, although the channel inside is
quite deep. The presence of this boulder barrier is probably due to its
deposition, in part at least, in a crack or rift in the glacier, that evi-
dently occupied the valley of the Blanche River towards the close of
the glacial period.

■ARLOW

THE OTTAWA AND LAKK TE.MISCAMIXG.

175 I

Tlie northern part of the lake, from the Old Fort Narrows to the
mouth of the River des Qiiinze, has more tlie appearance of a lake than
any portion further south. The deepest water is to the west of Mann
and Bryson ishmds, and is the route usually followed by the steamer.
At ordinary summer level it is impossible for a steamer drawing six
feet of water to pass between iJryson Island and the Quebec main-
land, and the lake for a long distance outward, opposite ^\'ri^■ht's
mine, is comparatively shallow. Kelly, or, as it is no'.v called,
Priests ]^ay, where the chief settlement of the disti'ict is situated, pre- I'lMcsts Bay.
sents a long stretch of gently sloping clay ilats, extending out from
the shore opposite the village of Eaie des Peres, and, usually, towards
tho end of August and in the month of September there is not more than
five feet of water at the end of the long wharf, so that for a consider-
able portion of the season the steamers ai'e compelled to anchor fully
half a mile from shore, and lighter their passengers and cargo.

The north shore of the lake is divided into two deep bays by the Noitlicrn
high rocky promontory termiiaating at Dawson or Wabis Point. The
high limestone tat lv.'-land of which this forms a part, is over two miles
in width, presenting a very steep escarpment of light cream-coloured
limestone facing eastward and running in a N. Is . W. dii-ection beyond
the borders of the map. Wabis Bay is a little over two miles wide Waliis I'ay.
and three miles in depth, receiving at its head the waters of Wabi Creek,
at the mouth of which is situated the promisii>g settlement of Liskeard.
Wal)Is Creek is a stream of considerable importance, rising beyond the
north boundary of the map and draining a large area of arable land to
the north-west, most of which has recently been laid out in townships
and sulidivided into lots. The borders of Wabis Bay are in general low,
with a marshy fi-inge along its north-west shore, while the water is
extremely shallow and the shore difficult of approach except by means
of the very crooked and narrow channel which the stream has hollowed
out on the hard clay bottom. The north-eastern part of the lake is North -eastern
divided into two bays known as Sutton and Paulson bays, separated ^^^'
from one another by the low uuirshy delta marking the mouth of the
Dlanche and Quinze rivers. The greater portion of Sutton Bay is a
low sandy flat almost completely dry at low-water.

When the lake is at its ordinarx' summer level, there is scarcely a foot Shallows near
of water covering the extensive clay flats in the vicinity of Chiefs Island
except in the various channels which the steamers entering in this
vicinity have hollowed out. During low-water, occurring in Septem-
l)er of 1887 nnd 1894. the greater part of these clay flats was exposed,
the water being confined to these comparatively narrow channels. Three

'hi

!' 1

• i: '

17G I

NIPISSINC. AND TEMISCAMING HKGION.

BARLOW.

]

Rivers

Blanche
Kivt'i'.

Navigable
part of ri\

The

large tributaries enter the lake in this neighbourhood and a fourth,
known as AVibika Creek, about eight miles in length drains the western
portion of the township of Guigues. The largest of these streams is
the one which really constitutes the upward extension of the (.)ttawa
River, now known as the Rivitre des Quinze or (Juinze River, The
other two, in the order of their importance, are the Blanche or White
River and the Otter River, often also called Ottertail River especially
on the maps issued by the Crown Lands Department of Qut;bec. Only
about five miles of the lower portion of the Blanche River is shown
on the Lake Temiscaming map-sheet, the source of the stream being in
Round Lake, is situated about f<jrty-four miles from its mouth
in a northwesterly direction, but following the rivei- the distance is
nearly sixty miles. The waters of the Blanche River enter the lake
through four somewhat intricate channels, between three low marshy
islands, formed by the large amount of loose niatei'ial deposited annually
by this stream. Two of these islands, known as Wright and Rousselet
islands, are of considerable size. The deepest channel is called the
Chenal du Diablo, and is navigable for small steamers at high-water.
The next channel further south is known as the Crow Channel and is
fairly deep, but the other two channels, which are more in line with
the upward course of the stream, are almost completely choked with
sand and other detritus, so that they can scarcely be nasigated by canoes
during ordinary stages of the water.

About five miles from its mouth, the depth of the river varies from
sixteen to twenty-four feet, and the width from 320 to 400 feet, and
at v, distance of twenty miles from its mouth it is 220 feet wide and
eight feet deep. [Tere a small rapid occurs, with a fall of about two
feet, but abo\e this is a quiet stretch of water for nearly six
miles further. It will thus be seen that, at low-water, the river is
navigable for a distance of twenty-five miles for steamers drawing
under three feet, while at its highest stage this distance is increased to
over thirty miles. The Blanche River has cut its channel through
a thick deposit of drift material, composed chiefly of clay, and
the sections thus furnished are probably the best in the whole dis-
trict. The valley consists of a series of four or five rather extensive
flats or terraces, rising, one above the other, to the north-west of the
lake, and evidently ft)rming the continuation northward of the depres-
sion occupied by Lake Temiscaming. Near its mouth, the l)anks of
the river are quite low, and subject to inundation, with large areas of
tamarac and spruce swamp. As the stream is ascended, however, the
banks gradually Increase in height, and thirty miles inland they are
more than one hundred feet above the \e\e\ of the stream. Twenty-five

miles fi
nisli a
two or
l)rown .'
clay, wl
stream,
of the r
lain by
again o\
theclills
of sand,

TheO

south-ea!

about si:

same dej:

channel i

of about

was meas

one half I

ond. It

about ten

in going t

from the r

of nearly

west of L<

erable lak

miles in le

mile, whi](

uneven sIk

breadth oi

River, dra

a small ma

is rather ci

tortuous m

The villa
origin, whi
considerabh
covered fiek

* Rejjort of
12

..]

TIIK OTTAWA AND LAKE TEMISCAMING.

177 1

miles from the lake, tlie banks are eighty or ninety feet high, and fia--
nish a good section, which is as follows in descending order : — First,
two or three inches of vegetable mould, then about a foot of reddish-
brown sand merging into a gray clay, and below this, again, a bluish
clay, which extends to the base of the clift', forming the bed of the
stream. Bluisli clay is exposed, according to ^IcOuat,* in the bed
of the river all the way to Hound l^ake, but about half-way up is over-
lain by a rather coaise, brown sand, which, in its tuin, furtlier up, is
again overlaid by clay. Six or eight miles below Round Lake, where
the cliH's are upwards of a hundred feet high, the middle portion consists
of sand, while at the base and summit nothing is seen but clay.

The Otter River drains by far the larger portion of the area to the Otter Fiivcr.
south-east of this part of Ijike Temiscaming. The main stream rises
about six miles south-east of Lac aux Feves, where it. occupies the
same depression as Chemagan and itay bays of Lake Keepawa. Its
channel is very tortuous, and in its lower portion has an average width
of about 100 feet, with a depth of ten feet, while its rate of cHscharge Its disdiarge.
was measured Ijy Mr. (luerin as 220 cubic feet pei' .second, or less than
one half that of the Blanche, and its velocity twenty-six feet per sec-
ond. It is navigable by canoe without interruption for a distance of
about ten miles from the mouth, and is frecpiently used by the settlers
in going to and returning from North Temiscaming. About six miles
from the mouth, tlie Cameron Branch enters, and, with a general course ' "^uiunm
of nearly east-and-west, has its head-waters in a small lake only a mile
west of Lac des Quinze. This tributary also serves to empty two consid-
erable lakes, known as Long and Sasaganaga, the former about three
miles in length, but with an average breadth of .scarcely a quarter of a
mile, wliile the latter is two and a-half miles long, with a .somewhat
uneven shore-line and containing several islands, has an approximate
breadth of a little over half a mile. The south branch, or Duford »'''>iitti 'inmcli.
River, drains the larger portion of the township of Duhamel, rising in
a small marshy lake about the centre of the township. Tliis stream
i,s rather crooked, even in its larger bends, while it meanders in a very
tortuous manner through clay flats.

'r\

ill

Geological jDescription.

The village of Mattawa is built upon a bouldery terrace of raorainic Bouklerv
origin, which, subsequent to its deposition, has been modified to a Muttuwli.
considerable extent by the scouring action of water. This boulder,
covered field or plateau has a somewhat uneven contour, but in general

* Reiiort of Progre.ss, Geol. Surv. Can., 1S72-7S, p. 134.

■'iii-

/:U '

! I

Character
liMiiUlers.

Terrace.

Mattuwa
Mountain.

Peguiatitf
dyke.s.

178 I

nip:ssing axd tkmiscaming kegion.

it may be .«aid to ri om thirty to severity feet above the river. It
is only one of many similar occurrences to be found in the neighbour-
hooil of the Ottawa River, all of which seem to owe their accumulation
primarily to deposition from a melting detritus-laden glacier. This
bouldery terrace begins nearly a mile up the Mattawa River and
extends a little over half a mile down the southern bank of the Ottawa.
In the angles formed by the junction of the two streams, it has its
ma.ximum development, producing a bar consisting almost wholly of
boulders and coarse graA^el, which stretches nearly across the river,
leaving a deep though nari-ow channel near the Quebec shore. The
boulders about jNIattawa vary in si/e from a few inches to as many feet
in diameter, while man}' of them measure from ten to fifteen feet
across. By far the larger number of these erratics consist of very
evenly folioted gneiss, and have not been carried far from their
original positions. iSome are f>f red and gray granite, while a few
are of greenish gabbro or diabasa, Recent cuttings show that
the bouldery layer overlies silts and other fine deposits. A well
defined old river-channel occurs, running through the rear portion of
the village between the main street and the railway station, which has
evidently been followed by the jNIattawa or its antecedent stream. It
leaves the Mattawa about a mile above the mouth, and reaches the
Ottawa at the foot of the rapid, nearly three-quarters of a mile below.

On the north side of the river, a steeply scarped though somewhat
narrow terrace rises to a height of nearly eighty feet above the level of
the river. Near the junction with the Ottawa this terrace is com-
posed of well-rounded fragments or small boulders with coarse gravel
and sand, this material being in a much finer state of division than that
on the south .side.

Oppo^:ite the village of Mattawa, on the north side of the Ottawa, is
" Mattawa Mountain," about GOO feet high. It is composed of a grayish
granite-gneiss, consisting of the usual alternation of lighter and darker
bands, causing a distinctly marked foliation. The strike of this folia-
tion corresponds closely with the trend of the hill, being nearly east-
and-west, while the dip is about 20° to the south. In places it con-
tains an abundance of rather smiill garnets, especially numerous in the
darker or more basic portions of the rock.

At many points this gneiss is cut by dykes of pegmatite, varying
irregularly in breadth from a few inches to several feet. These
pegmatites are compo.sed usually of a flesh-coloured orthoclase or
microcline and (juartz. Occasionally a white i)lagioclase, probably
oligoclase, was noticed in the same dyke with the orthoclase, while the

v.]

ness.

Till'; OTTAMA AM) LAKK TP.MISCAMINT;.

179 I

ferro-magnesian constituent is sparingly represented, if at all, and is
usually l)iotite. The quartz is a;; a rule segregated in the centre of
each dyke, leaving an almost pure felspathic margin of varying thick-
ness. Many of these dykes cut the foliation at considerable angles,
running from S. 40' W. to S. 55° W., while others, especially the
smaller ones, conform very closely to the foliation.

It is quite apparent, from the many conflicting local dips and strikes ( jneissos
observed in the area to the south of tlie Ottawa River, and extending f<"'"i'"K ^i""-'!
for a few miles east of Mattawa, that the gnoissic rocks rise into a series
of small domes, each presenting quaquaversal dips ; while, on the other
hand, the complete examination of this small area has also shown that
the grander structural features of these rocks exhibit a rather constant
dip at low angles, varying in direction from south to S. 10° W. These
gneissic rocks are well foliated and of a dark-gray colour where the
bisilicate material is present in relatively greater quantity, while a pre-
vailing reddish tinge is usual where felspar present increases. Some
bands exhibit the " augen " structure in great perfection.

About a mile east of Mattawa, the main line of the Canadian Pacific
Railway has cut through the axis of one of the most perfect of these
dome-shaped bulges. The gneiss occurs in alternating light- and dark
coloured bands which exhibit very sh «rp lines of demarcation one from
the other. The main axis of this dome runs in a direction S. 80° E
the dips on the north side of the railway track thus turning from N
80° W. all around to S. 80° E.; while on the south side of the track
dips exactly the opposite of these may be noticed.

The gneisses contain a large percentage of pyrite, and all the joints Character of
and fissures arc plentifully coated with brown hydrous oxide of iron K"^'''*'-
due to the decomposition of this mineral. The rocks crumble and fall
to pieces when exposed to the action of the atmosphere for any length
of time, giving rise to a coarse brownish sand that constitutes much
of the soil of the region surrounding Matta'va.

About a mile and a-quarter oast of Mattawa, the gneiss has a dark Suiierficial
reddish-gray colour, the reddish tinge being due to the presence of
felspar, which is in reality much more abundant in certain bands than
in others. On the surface the gneiss presents a smooth hard crust, that
is evidently merely the result of weathering, while beneath this thin
coating the rock has undergone somewhat advanced decomposition, being
yellowish in colour and comparatively soft and friable. This outer in-
duration is very frecjuently chai'acteristic of the exposed surfaces of both
gneisses and the Huronian sandstone and greywackes, and, as has been

i Hi

! !

I i

180 I

Nll'ISSIXfi AN'I) TEMISCAMING UKOIOX.

iiock

bitw

■I'll

tiiwu

iUK

(

vili.

Sti ike

\VC.~t I

tiiwa.

Strike
Rapids

shown Ijy Trviiif,' and Van Hiso, is caused l)y the secondary onhirj,'e-
meut of the i|uart/ and felspar individuals, the interstitial material
constituting interlocking areas which arc optically continuous with tlie
original grains.

To the west of ^Nlattawa, the railway follows up the valley of a creek
tiiat empties into twD small lakes, the larger of which is known as
Eai'ls Lake. The shores of both these lakes are low and grassy, with
only one rock exposure at the western end of Pearls Lake. Between
Matiawa and Calvin stations the rock is usually well foliated
granite-gneiss, althougli in one or two places it is very massive, and
the foliaiion is uther absent or (|ui(e indistinct. Some of the bands
dilTer in colour from dark-gray to almost black where the biotite is
exceptiunally abundant ; others are light-gray, while still otiiers are i>f
shades ot llesh-ied or pink wheni the felspar is plentiful and is of that
colour. The component bands are fro([UPntly so irregular in their
development and in jjlaces so contorted, while the region as a whoh;
hcas undergone such uneven truncation, that it is often e.\ccedinL,ly
dilticult to i>ronounce with any degree of certainty as to the
direction of either the dip or the strike. In general, though, these
rocks giadually bend round from S. 45' W. a littleVost of ^lattawa, to
8. 80 W. in the vicinity of Calvin, with a connnon dip at a higli
angle to the south. One of the pegmatite dykes, noticed about two
miles west of ^lattawa, is composed of a very large quantity of llesh-
red felspar in coarse cleavable masses, some fjuartz and a considerable'
amount of dark-coloured mica, in large crystals and plates, doubtless a
partially bh-ached biotite. All of the rocks are well rounded and
glaciated, and although the strife are not very phiiidy marked, some
indistinct ones have a south-west direction, and ai'e thus referrablc to
the period of general glaciation.

In the angle formed Ijy the junction of the ]\lattawa and Ottawa
rivers, and to the north and east of these streams, the foliation of the
gneiss shows a curious fan-like arrangement, the convergent lines
pointing towards the Ottawa, where the gneiss shows a rapid change
in strike from nearly east-and-west at the southern end of the rock
exposure to N. 2")° W. at the northern end. This structure is, how-
ever, only a local feature, and is con lined to a small area. To the west,
this fan-like fi^rmation broadens, he bands near the southern end
curving round rather sharply to the south-west to meet those exposed
on tie shores of Boom Lake and in the vicinity of the Plain Chant
Rapids on the Mattawa, where the gneiss strikes from S. 30' W. to
It Cue S. 60" W. with a south-easterly dip < 40° to 45°. To the north, as the
Ottawa liiver is ascended, on the west shore the strike of the gneiss

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13 WiSTMAiNSTRiET

WEBSTIR, N y. MSSO

(716) S73-4S03

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chan
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l;i III

THE OTTAWA AND LAKE TEMISCAMINO.

181 I

changes first to the west and then to N. 75° W., which latter seems to
be the general direction of the foliation in the vicinity of the Cave
P ipids. At the bluff on the east shore, the rock is composed of alter-
nating bands of light- and dark-grtay micaceous gneiss, e.idently of the
ordinary granitite variety, and shows a strike of N. 55° E. and a dip to
the south < 10°-15\ Above this again the foliation exhibits a change
in direction, and about three-tjuarters of a mile below the Cave Rapids
a strike of S. 75 E. was noted, with a dip southward < 20. A little
above the rapids, the evenly foliated gray gneiss trends in a north-
easterly direction, dipping to the south-east < 30\ Between the Cave
and Les Eraljles Rapids, the granitite-gneiss, which in the more basic
bands seems to contain some hornblende in addition to the biotite, varies
in strike from S. 70^ W. to N. 70' W. witli a soutiierly inclination.

Les Erables Rapids are caused by the outcrop of ledges and islets of At L«s p;ra-
gneiss, which obstruct an already much contracted channel. The strike "" "''"^■■'"
is N. 70' W., while the dip is northwards at an angle usually con-
siderably less than 10'. A little above these rapids the foliation has
an almost east-and-west direction, while near the mouth of Snak<^ Creek
the strike is N. 80 E., and the dip 8. < 70 . From the head of Les (jmissps

Erables Rapids to about half a mile beyond the mouth of Snake Creek, cmtuining

' '' . clyaniK'.

the exposure'^, which wore \ery closely examined, show a gneiss com-
posed of alternating bands of light- and dark-gray colour. The bisilicate
present, which, from its preponderance, gives the dark colour to cer-
tain biuuls, is biotite, and the rock is thus a granitite-gneiss composed
essentially of felspar (chiefly orthoclase), quartz and biotite. Besides
these constituents, there are others, which in places are so abundant
as to characterize the rock. The principal and most interesting of
these is cyanitc, although individuals of an almandine-garnet are
usually numerous, especially in the more basic portions ; while giaphitc
was noticed finely, though rather thickly distributed through the rock.
Cyanite of a prevailing blue colour is frequently so plentiful as to char-
acterize large exposures of this gneiss. It occurs in rectangular or
llattcnf d prisms, which are very long and blade-like in their lialnt,
presenting round, jai.'ged, or irregular terminations.

About a mile below The Mountain Rapids, the high hills on the east R,,(•k^l noar
shore are formed of alternating bands of light- and dark-gray yarnetif- J'"' ■)I""">''ain

'^ ° . O J P Kill>|ll.S.

erous granitite-gneiss, striking S. 55 W., and dipping south-easterly
<'15 toG0°.

At the foot of the Mountain Rapid, the gneiss is more massi\ e in
structure, although still preserving a distinct foliation that runs
nearly east-and-west, while the dip is to the south < 35 to 40. In

■-■*
1

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I lit.

i:il

I i

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Ill

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182 I

NIPISSINO AND TKMISCAMING KEOION.

A1k)V(' the
Kill litis.

At narrows of south
Seven Ltagiit
Lake,

On noitlicrn
part of hike.

Rocks

liftwefii

Ldiitr Siiiilt
and LaUe
Keepawa.

places it is filled with small crystalline or irregular fragments of gar-
net, while the rock in general has a distinct reddish colour. The
jNIountain Rapid runs for the most part in the strike of the rock,
which is a dark-gray, well foliated gneiss. The ridges and islets are
composed of this gneiss, presenting a strike varying from S. 50' E. to
S. 5')" E., with a dip to the north-east < 20' to 30'.

About a mile above the Mountain llapid, on the west side, the
dark-gray, niicaccoiis or granititegiu-iss strikes S. 70' W., with a dip
to the south. About one and a-half miles above this point, a gray
gneiss was noted with a decided foliation, exhibiting a series of beauti-
ful curvings and *wistings, while the general strike is N. 60' E.,
with a liip to the south-east < (15 to 70^. About four miles above the
IMounlain Itapid, a massive, tine-grained, red gneiss was noticed, asso-
ciated with some more evenly foliated, gray gneiss ; the whole dipping
40-80'. In the vicinity of the narrows of Seven League
Lake, and for some distance beyond, the gneiss is in many i)laces much
contorted, and usually of a dark-gray colour, owing to the prevalence
of the mow basic liands. In many places the rock runs in long cur\es,
presenting a gentle undulating dip, which often approaches horizon-
tality, while at other points not far removed the bands are almost on
edge. lieyond the narrows on Seven League Lake, the gneiss, which
has a gray colour and is well foliated, strikes about S. 65 E., with a
southerly dip at a low angle, generally from 20' to 30°. Opposite La
Tuque, on the east shore and below the mouth of Obashing Creek, tha
lighter coloured bands, which are reddi><h, alternate with those of a
dark-gray. These constitute a granitite-gneiss, which generally dips
8. 25 AV., • ; 10 to 20', although in some places it seems perfectly horiz-
ontal, and in others it is much contorted.

At the foot of the Long Sault, the n.'ddish granitite-gneiss dips S.
20° VV., < 25". In many places along the shores of the northern part
of Seven League Lake, the darker and more basic bands of gneiss con-
tain epidote in very considerable quantities, indeed sometimes so
abundant is this mineral as to givi; a yellowish tint to the band in
which it is contained.

The country between the Long Sault Rapids and Lake Keepawa, is
composed of high, rocky ridges of ilesh-red and dark-gray gneiss, the
former prevailing, while the alternation of both produces a marked
foliation iii the whole mass. The ilarker bands are made uj) mostly of
the coloured constituents, while the lighter ones show a relatively
greater quantity of quartz and felspar. Tlie general strike varies from
S. 50° E. to S. 60" E., while the dip is under 30'. A thin section of

'4i

'■'l

.1.

10*1

TilR OTTAWA AM) LAKE TKMISCAMINO.

183 I

what was regardod as a typical specinu'ii of this gneiss, sliowed it to
be a <juartz-inica-diorite-},'neiss, ahliouj^li it is prohable that other and
inorc^ acidic port ions would show the ordinary granitite-gneiss, as well as
the hoiiiblcmle grunititu-grieis.s, to be present. The rock, as examined
under the microscope, showed the chief mineral constituents to be
plagioclase, quartz, some unstriated felspar (probably orthoclase) and a
little microline, hornblende, biotite and epidote, with smaller quanti-
ties of titanite, pyrite, zircon, allanite, apatite and hrematite.

On the ]>ig Oltashing Lake, the gneiss is usually well foliated, often OnObasliinj,'
ova light-gray colour, although some portions present • eddish-coloured
l,>!inds where the fclspai" contains much iron oxide, and the general
strike in the vicinity of the narrows varies fi'oni S. GO E. to S. 75'
E. with a dip to the south < 15 to 30°. A.t the east end of the little
island in the ba}- out of which the road goes south to the small lake at
the hcad-watci's of Snake Creek, the gneiss is conijiosed of alternating
reddish and dark-grey bands, in filaces somewhat contorterl, and shows
a general stiike of S. 85 Vl. with a dip to the south < 7C to 80 . Near
the east end of Obashing Lake, the dark-gray well foliated gneiss strikes
S. 8-1 E., and is either ijuite vertical or dips at a very high angle to
the south.

>iear the outlet of Little Obashing Lake, the gneiss, which is distinctly
foliated and has a reddish colour, strikes east-and-west, dipping south
at an angle of about 35". The suialler lakes to the southwest of Little
Obashing Lake, generally present high shores which are well wooded
and green to the water's edge, so that there are only limited opportuni-
ties afforded for ascertaining the trend of the bordering gneiss. On a
small island in Thompson or ^IcConnell Lake, however, gray gneiss was
noticed dip})ing S. 20 W. at a low angle.

Xear the head of the Long Sault, on the west shore of the Ottawa, n .i. f,.,„„

the ''neiss is composed of alternatin'' li'dit and dark bands. Many of ''""K ■'^;'»lt
' 1 til U],iiiiika

the lighter bands have a flesh-red colour where the felspar is abundant, XanuWH.

while others are grayish or nearly white. The dip is S. 30' W. < 20 .

There are comparatively few exposures of rock between the head of
the Lang Sault and the Opimika Narrows, and the strike at some of
these is hard to ascertain witii any degree of certainty. The general
strike seems, however, to be S 55' E., which is apparently maintained
as far as Schooner or Ship Island. On the east shore, opposite this
island, the gneiss, which is exceedingly well foliated in alternating
bands of light-gray ileshred aiul dark-gray colouis, dips S. 10 "W,

< m.

■i
i; ■ ■

i r

184 I

NIPISSIVa AND TEMISC/VMINO REGION.

'? i!

Curving
utrikf I if
fuliatiun.

Region

8imth-\vcst ■
C)|iiiiiik:i \
rowH.

Region
nortti-wcst (
Opiiuika N
rows.

To the south of the Opimika Narrows, on tlie west side, and nearly
opposite Luniaden's depot (Opimicong P. O.) is u gray, ratlier fine-
grained, evenly foliated micaceous rock, showing lenticular areas of
quartz and felspar which are comparatively free from coloured consti-
tuents. The microscope shows the rock to be a hornblendegranitite-
gneiss composed chieHy of quartz, orthoclase, plugioclase, microcline,
biotite and hornblende, whith smaller quantities of ilmenite a.ssociated
with leucoxene, sphene, apatite, calcite, zircon and epidote. The dip
of this gneiss is S.W. < 45 .

This exposure marks the southern end of a great curve in the gneissic
rocks, the Opimi'-a Narrows conforming closely with the strike of
the rocks in their bend. At the southern end, the strike is north-west,
about half-way through it has changed to S. 75 W., at the north end
of the Narrows the strike is N. 15" W., while still further north on the
same side it bends around to N. 30' W., and near the mouth of
Ottertail Creek the rock strikes N. 35'^ E.

The gneiss, in this interval, is of the usual gray micaceous variety,
occurring in alternating light and dark bands, while the dip is to the
west or north-west at high angles, usually about 05°. A thin section,
cut from a specimen obtained at the exposure innuediately below the
mouth of Opimika Creek, showed the rock to be a gianitite-gneiss,
composed chiefly of quartz, orthoclase, plagioclase and microcline, with
biotite, epidote and sphene as its principal coloured constituents.

In the region to the south-west of the Opimika N.arrows, the country
is well wooded, and the few rocky outcrops encountered have a
general south-westerh' strike. Near the small bridge on the old
McLaren lumber road, crossing Opimika Creek less than a mile
from the lake-shore, the gneissic rocks are very evenly ami distinctly
foliated, showing intcrlaminations of reddish light-gray and dark-gray
material, the whole having a strike of nearly north-and-south and
dipping west ' 20 . Two miles south-west of the lake, other small out-
crops of a light-gray granitite-gneiss occur, dipping S. 50 W. < 35^
Near the end of McLaren road, the rock is concealeil for the most part
by sand, but here and there hutnmou'ks of gneiss occur. One of these,
situated about tliree-(iuaiters of a mile from the end of the road is
composed of gray well foliated gneiss dij)ping S. 80 W. <20'.

To the north-west of the Opimika Narrows are situated Long and
White lakes, which empty into Lake Temiscaming a short distance north-
west of Lumsden's depot. These lakes are noteworthy as affording an
opportunity of ti-acing in some detail the genei'al outline of an immense
curve in the strike, that, starting at the south end of the Opimika Nar-

rows w
Beauvi
compo.s
which
the lay«
the lak(
On W
the nor
west.
gneisse.s
iiig sout

On tl
very pli
long slei
portions

BARLOW

THE OrfAWA AND LAKK TEMISCAMINO.

185 I

rows with a direotion N. 40' W., circles arouiul to S. 65° E. at the
Beauvais Narrows on I'vke Keepawa. On Long Lake, the gneiss is
composed of successive bands of reddish-gray, gray and llesli-red colours,
whicli vary in strike from N. 20" W. to N. 7 W., wliile the attitude of
tlie hiyeis changes from nearly horizontal in the south-western pait of
the lake to an inclination to the west of ;)5° in the north-eastern part.
On AVhite Lake, the rocks curve around gradually to N. 53 E., and on
the north shore the gneiss lias a strike of only a few degrees south of
west. These rocks are light-red, reddish-gray, light-gray to dark-gray
gneisses, the layers running in low, broad undulations with a prevail-
ing southerly dip at angles varying from 5' to 10^

On the north side of White Lake, there is a reddish contorted gneiss On Wliite
very plainly foliated, a ferroniagnesian constituent being present in
long slender dark-grecjnish bands, while in the wider and more felspathio
portions such coloured constituents are almost entirely absent.

To the north-east of McMartin Point, on the portage going to White On jwrtatre to
Beaver Jjake, the gneiss is exceedingly well tohated, running in long Lake,
generally straight and somewhat continuous bands of alternating liglit-
and dark-gray colour and varying in strike from N. 40' 8. to N. 50 E.:
with a prevailing north-westerly dip at high angles generally about 75".
Exposures on the south shore of White Beaver Lake exhibit a light
reddish-gray gneiss in successive bands of lighter and darker colours, the
whole showing a changeable strike from N. 60" E. to N. G8'' E., while
tiie folia arenevrly if not quite vertical.

B(!tweon McMjirlin Point and Latour's mills, the east shore of Lake Of cast slmro
Tmnisciining is very high and precipitous and for considerable stretches j'jj"' •\',\^^f'
presents perpendicular rocky clifls. For two miles above McMartin
Point, the gneiss is compaiatively massive and chielly of the red
variety, although gray bands may be noticed marking the foliation.
This rock has, in general, a dip N. 65' W. < 35° to 80'. The com-
liined action of the weather and tlie waves of the lake have served in
many places to remove an appreciable portion of the softer and more
micaceous bands, leaving the red felspathic parts standing out in
rather prominent relief, smoothed and planed as a result of glacial
action. The surface now exposed exhibits, in great perfection, even the
smallest bendings and foldings which these rocks have undergone. In
the last half mile of the distance already mentioned, the gneissic rocks
seem to strike approximately with the trend of the shore-line, exhibit-
ing beautiful examples of contortion, while in other places the rock
lies in a series of low undulating folds. Above this, for a little over
four miles, and extending a short distance beyond Latour's mills, are

» :'

'■;

18G I

MJ'ISSINli AND TKMISCAiMINU UK(iION.

I '! ! ■ (

MIM

iij'i

Of west si Idle
near MrMar-
tiu I'uiiit.

Rocks o|ii)o-
siti' riiitiiiirs
mills.

Jiu'hisions ill
gneiss.

almost contiiiuouH exposurtis of inicafpons or <j;ninitito-f.;rn'iss, which
i.s so ovfiily !;iminiitiHl tlml. slabs could readily be oblained of
almost any dimensions for tlaj^stoiu's. The strike is vtny regular,
generally about N. 15' E., and the dip easterly < 50° to 80". The
alternating liands composing the gneiss are usually rtildish, grayish
ami dark-gray in colour.

On the western , h ore, for a short distance liotli above and below
Mc .Martin Point, the rocks are somewhat similar in character, the
strike varying from S. 3.")' W. to S. iU) \V., while the inclination,
which is towards the north-west, changes from an angle of G5 to 3."i .

About a mile ajove Mc?ilartin Point, on the west shore, the gneiss
is nnich contorted, and in oiit^ place presents a low. dome-shaped
anticlinal arch, the banding of the gneiss dipping either to the
north west or south-west at low angles. Nearly two miles above
McMart in Point, or ten miles .south of the mouth of the Keepawa,
the gneiss is made up of alternate layers in w Inch a relatively greatv-r
amount of fels'^u- and quartz or biotite and hornl)lende are
respectively present. The darker bands have yielded somewhat
extensively and unevenly to atmospheiic decay, the felspjithic layers
standing out in rib-like forms. The strike is chietly to the south-
east, while the bands have either an almost, vertical attitude or dip at
high angle, never less than 70 , in a south-ea.sterly direction.
l\'icroscopical examination of a specimen representing the more basic
portion of the rock, shows it to be a iiuart/.-mica-dioriltvgneiss, com-
posed essentially of j>lagioclase, orthoclase, quartz, hornblende, bititite
and ejiidote, with sphene, apatitt> and zircon as accessory constituents.

Opposite Latour's mills, and for a short distances both north and
south, the gneiss is well laminateil, exhibiting precisely similar
features to that on the opposite; side of the lak(\ The felspathic bamls,
which are usually ileshred, are rathei- line-grained and contain little
quartz or mica, while the darker bands show a superabundance of
biotite and other ct)loured constituents.

In several places, associated with this gneiss and evid(>ntly caught
up in it, are irregular masses of a dark -green, almost uralitic diabase,
with somewhat largo and glistening scales of dark-lirown mica. The
surface of this rock weathers very unevenly, presenting a very rough
and pitted character. This roughness is increased by a series of intri-
cate, reticulating dykes of a line-grained aplite or granite that stand out
in strong relief. Under the microscope, the rock is seen to be an
altered diabase, the hornblende showing uuiloubted evidence of Inning
been derived from pyroxene, while traces of a rude ophitic structure

TIIK OTTAWA AND LAKT. TK>IISCAMIX(i.

1S7 I

Cllll s

till

)0 (lotoctod

K* Other iiiiiu'ials jxesent iire hiotilc, j)la>;i

clase, garnet, and iron ore.*

l>oLweeii Liitour's mills and the western end of the old Indian port •
age-route to Lake Keepawa, the gneiss is not so regular as that further miiis.

(in kn llOltll

sou

th,

and in some places runs

par

allel with the shore-line, while at

others it forms considerahle angles with this direction, makin<r at least

one areat bend, which is shown on the ac

company nig map.

The rocks are either vertical or dip at high angles to the east and
south-east. A little .south of tlie Indian portage, there are some dark-
green, almost black, glistening bands of amphibolite, which occin* fur Aiii|iliilHilitc.>
the most part interfoliated with the prevailing gnei.ss. These pre.seni
many of the characteristics of paifillel or interfoliated dykes, and snnu'
jiiirlions of them cut across the foli.iiion, but their true relations won-
not studied in detail, so that it cannot Lt stated with certainty whether
tluy are of later origin than the gneiss with which they are associ-
ated. Tlu^ micrt)scopic examination (tf two thin sections .shows tluit,
although it must bo referred to as nuartzinica-dioritegneiss, it dillci's
in many particulars from the basic bands of the ordinary gneiss to
which this name has also been applied. It has very evidently been I'ludiutd liy
(lerived from the shearing of a basic eruptive rock, resulting in lis ^ "''""'*^'
more or less complete iv-crystalli/ation, and seviMal places weio noticed
throu.;hout the regit)n where a similar rock could be traced dii-ectly and
continuously into the ordinary massive phase, which for sonn; reason had
escaped such complete deformation. ( ine of the localities where this
can })erhaps be seen to the best advantage, is on the shores of one of
the smaller bays running to the north-west, and forming part of Leon-
aid Inlet, on the west coast of Shabosagi or Wicksteed Lake. This
amphibolite, or (piartz-miea-diorite-gneiss, is composed of quartz, j)lagio-
clase, hornblende, with an iron ore (probably titaniferous) and epidotc,
g.irnet, apatite and zircon. Associated also with the gneiss near this
point is some of the uralitic diabase already described as occurring on
the west shore of the lake.

From the Indian portage northward to within about two miles of Ivist sliuic,

iinrtli to Ml
ll'4ill JiiviT.

the mouth of the Montreal River, the rocks pre.sent the usual alterna- "'"''' '" *^'"""

tion of reddish, gray, and ahnost black bands. The strike of the folia-
tion is somewhat irregular or divergent, but the general directions are
indicated on the accojupanying map.

Alartel Point, as well as the shores of the small bay to the south, and
some small rocky islets lying close to the eastern shore of the hike in
this vicinity, are composed <jf a dark -green, ahnost black diorite.

* S(;ctiuu No. 58.

''%

■^ h

rnW

188 I

NiriS.M.NV; AND TEMISCAMlNc; KKUIOX.

Wist >lic>p'. From lUilValo llock nortliwanl.s along the west shore, the strike of

tlie gneiss docs not show any wi(h> variation, the lioneral direotion
being from S. 4o \S'. toS. 05 W. with a dip to the south-east c^ 40 to
80'. The general colours are shades of light- and dark-giay, with some
reddish l)ands where the felsnar has been stained by iron. A specimen
obtained tVom ^m exposure noai'ly opposite the mouth of the Keepawa,
siiow.> a tint'-grained, gray, evenly foliated, micaceous rock, slightly
discoloured throughout by iron oxide. The microscope shows the rock
to be a granitite-gneiss, consisting chiefly of orthoclase, cpiartz, biotite
and epidote and bearing a close resemblance to the gneiss exposed near
the north end of the Opiniika Narrows, although somewhat liner in
texturi'.

('Miitinr nf The contact between these gneissic rocks, m.apped as i^aurentian,

Luuciiiiuii 1,11 • 1 ■ 1 •1111

and Iliiidiii^iM. and the lluronian locUs, is exposed on tiie west siiore ot tlie laKeal)out

two and :i (piartcr miles south of the mouth of the Montreal River.

hniiu'diatcly south of the small crock wiiich enters the lake from the

west four and a half miles snuth of the Montreal l'i\er, the gneiss has a

strike of S. GO W. with a dip 8. 'M E. <^Sb', while in the bed of the

creek itself the rock is a])pareiitly of a coarse (hirk micaceous variety,

decomposed ahmi.st whiilly In a chlorite-schist associated with some

steatite or .soapstone. l"or nearly a mile north of this, the shoi'e is

comiMiscd of a tlcsli-red giici-;sic granite, striking from N. GO W. to N.

70 W. and clipping to the south-wesL at high angles The point about

a mile to the south of the contact is occui)ied by a m:issive dark mica-

diorite or uralitic diabase, inlersected in \arious diicctions by dykesof

red gneissic material. Neai' the junclion the Laurentian is repi'csonted

by a light i'(>d(li-h or reddish-gray gneissic graniti-, with somewhat

iniliNtinct foliation l)ut no lamination. TJie I'ock is ma--sive, rather

coarse-gi'.-iincd, containing a comparatixi'ly small pro[ioi'tion of hisilicate

mateiial. I luler the microscope it is st^en to be a graul' ite-gm-iss, the

felspar having undergone somewhat advanced saussuriti/ation, wliile

the biotite originally piesimt has been wholly con\erted into chlorite.

I'lViMciacviii-
gloiiicrati' at
tlic contact.

Contiiiiiod
fi'atirini'nt.-!.

The rock in contact with this gneissii; granite on the wi>st shore
representing the lluronian, is the typictil and widespretid lireccia-con-
glom(>rate described by Sir William Logan as "shite conglomerate" or
"chloritic .slate conglomeiate".

This rock contains numerous angular as well as rounded fragments,
among which those of a somewhat coarse tlesn-reil granite are the most
abundantly re])res(mted. These granite pebbles ;ire composed chiefly
of (lesii-icd orthoclase, with a smaller (|uantity of grayish translucent
quartz and relatively little biotite, which has evidently undergone very

• u

i i#

■ *■

II!

advanced
rock wliic
were noti
chiefly (|U
tal iiiatei i
epidoto ai
and inatri
The coars
to tlu' lilK
curves arc

The gni
together a
it not for
pieces exh
of contact
direction
granite ha
siniihir irr
ate. It is
tliat they
rocks witli
posing the
a deeper n
exposed on
Besides, tl
often conti
similar roc

The Hui
the lake, is
generally c
a specimen
of the rivei
occasionall;
microcline,
division, w
smaller int
like in chai
or conchoid
dipping S. I
developed s
north of tl:

TIIK OTTAWA AND I.AKi; TKMlHrAMINfi.

189 I

advanced alteration to chlorite. Occasional specimens of a dark-green
I'ock which seems to be an extremely fine-grained and altered diabase,
were noticed, while irregular and angular fragments of simple minerals,
chiefly (|uart/. and felspar, are rather abundant. This coarse fragmen-
tal material is held in a dark-green slaty matrix, in which chlorite and
epidoto are the most abundant constituents, llolh the larger fragments
and matrix have been subjected to intense and long continued pressure.
The coarser fragments are .scjueezed out in a direction at right angh'S
to the line of junction, while the softer and more yielding matrix
curves around these inclusions.

The granite iind conglomerate are very closely and firmly cemented Aotnal lino of
together along their line of junction, and it would be (juite easy, weii- J'""-'*"'"'
it not for the broken and jointed character of both rocks, to .secuii'
pieces exhibiting portions of each in the same band specimen. The lini-
of contact in the immediate vicinity of the lake runs in a general
direction of S. 7*)' W., but this line is not jjcrfectly straight, ns the
granite has a somewhat sinuous edge which is followed '.ery f ilthfully by
similar irregularities in theschi^'^^c structure of the breccia-conglouv^r-
ate. It is (juite e\ ident from an inspection )f the coarser fragments
that the}' have not l)ee.. Jerived from the disintegration of the gneissic
rocks with which these elastics come in contact, for the n)inerals com-
posing them aie 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 the Old Fort Narrows.
Besides, the rock in immediate contact with these Laurentian gneisses
often contains far fewer fragments of such matei'ials than exposures of
similar rock farther removed from the line of junction.

The Huronian to the south of Montreal River, on the west shore of (^Immctir
the lake, is as a rule represented by a fine-grained felspathic sandstone, |I,,.,,.'\'i','!,\'t'J',.^]
generally of a pale greenish-gray colour. ]Microscopic examination of If'vtr.
a specimen obtained about a mile and three-cpiarters south of the mouth
of the river, shows this rock to be made up of angular, sub-angular and
occasionally of rounded fragments of orthoclase, ([uartz, plagioclase and
mierocline, cemented together by similar material in a finer state of
division, with some chlorite, epidote and serecite often filling in the
smaller interstices. In many places this rock is very hard and flint-
like in chanacter, breaking readily under the hammer with a splintery
or conchoidal fracture. It occurs in somewhat thin beds, often shaly
dipj)ing S. 83° W. •< 20° while a set of cleavage planes which havti been
developed as a result of pressure dip S. 20° E. <^ 70°. At the point just
north of the contact, the rock is a greenish-gray compact slaty grey-

;

i! :.

A-

190 I

NIPISSINC. AND TEMISCAMINO REGION.

°^ti'

!•:,

East shore,
north (if Mar-
tel I'oiut.

Character of
breccia-con-
glomerate.

wackt', wliich has evidently been subjected to gnat pressure and alter-
ation, for a distinct foliation or chistose structure has been developed,
the various Ijands of the rock being squeezed out into lens or pod-shaped
areas, while pronounced curves in the direction of the schistosity may
be observed, due to the unequal resistance (loforniation offered different
bands and portions of the rock. At the immediate line of contact the
parallel structure of both Laurentian and Huronian coniform with one
another, these being produced as a result of mutual reaction, the resist-
ance olVered by the neighbouring clastic primarily determining the direc
tion of foliation in the granite, while the forces of upheaval in the
gneiss have served to compress very materially the neighbouring clastic
rocks. The Huronian strata which are here present, form a curiously
lengthened wedge-shaped strip between the Laurentian granite and the
laccolitic or overflow mass of diabase which constitutes the summit of
the " King of the Beaver."

On the east shore of the lake, from Martel Point northward, the
Laurentian is represented almost altogether by a pale tlesh-red granite,
showing little or no bisilicate material, the principal coloured con-
stituent being epidote, which is somewhat abundant. The contact
between this rock and the breccia-conglomerate of the Huronian, is, on
the east side of the lake, about three miles north of the jNlontreal River.
The actual contact is concealed, but outcrops of both rocks occur within
a space of less than one hundred yards and from these it would seem
that the line intersects the shore at a point immediately south of a
small creek which empties into the lake in this vicinity. Inland, the
line is effectually hidden by overlying drift material, but its general
direction seems to be very approximately N. 55' E.

The granite near the contact contains a large irregular mass of a
coarse dark-green diorite. An area of finer crystalline chlorite-schist
runs at right angles to the line of junction, and may represent either a
small basic dyke which has been subjected to pressure, or an extremely
altered fragment of the Huronian greywacke which has been caught
up in tlie granite.

In the breccia-conglomerate the matrix is often present in very sub-
ordinate (juantity. The most abundant fragments are of the usual
biotite-granite type, while others of a pale grayish granitic rock, are
seen in thin sections under the microscope to consist of phenocrysts of
plagioclase or orthoclase imbedded in a fine-grained quartz-felspar
groundmass. Besides these, there are some fragments composed of a
tine-grained altered diabase and others of a greenish-gray slaty rock
(resembling in a most marked manner the compact variety of the grey-
wacke of the Huronian) and some gray quartz.

v.]

THE OTTAWA AND LAKE TEMISCAMING.

191 I

The material filling the interspaces is seen under the microscope to Stratificntion .
consist of a confused aggregate of scales and grains of chlorite and
epidote, with abundantly disseminated particles of iron ore and fine
granules of sphene and epidote. At first sight this conglomerate,
occurring as it does in very massive beds, with no pronounced parallel-
ism in the arrangement of the larger fragments, seems devoid of any
definite structural features, but a closer inspection shows the strike to
he about N. 50° E. while the dip is to the south-east <10°. As here
exposed it forms a hill about four hundred feet in height, presenting a
very sharp and abrupt northern face, while to the south it slopes more
gradually down towards the line of demarcation between the two
formations. To the north and west, this rock is succeeded by a dark
greenish-gray, compact, slaty rock which seems to underlie the breccia-
conglomerate, although in other sections the conglomerate occurs at the
very base of the Huronian. The exposures at this place, however, are
not in immediate contact, so that the relations of the two could not be
ascertained with certainty.

On the small island in Lavallee Bay, the rock is a fine-grained. Rocks on
greenish-gray greywacke, much squeezed and jointed, breaking with a
conchoidal and somewhat splintery fracture. The small island near
the east shore about a mile south-east of Roche McLean is also formed
of a similar greenish-gray compact felspathic sandstone rather massive
in structure.

■;

■ 'r "

The western shore of Lake Temiscaming, from the Montreal River
to Roche McLean, is occupied by the massive, bedded, breccia-con-
glomerate which dips in a westerly direction at an angle of 15° This
rock has already been described. A specimen obtained from an
exposure about two miles north of the Montreal River^ however,
showed the matrix to be relatively more abundant than usual. The
diabasic pebbles are also more plentiful than those of red granite,
while fragments of simple minerals predominate greatly over those of
composite rocks. The quartz and felspar fragments are sharply
angular, while the composite individuals are as a rule somewhat
rounded.

In the conglomerate near Roche McLean, the pebbles are more
rounded and much more sparsely disseminated through the matrix.
Pieces of an extremely altered diabase were noticed and also some of a
fine-grained greatly crushed quartz, filled with small scales of aerecite
and chlorite. The reddish pebbles are of the prevailing type of
biotite -granite or granitite. Roche McLean itself is a large rounded
and glaciated hummock of this breccia-conglomerate, separated from
the west shore by a narrow interval at high water.

West shore
Montreal
HivHv to
Roclie
McLean.

I ;

-■!;

•in ';

I , ■

192 I

NIPISSING AND TEMISCAMINO REGION.

West shore,
north of
ilurUe
McLt'ivn.

Isliind Point

Spotti-d
granite.

(Jul tin Puint

To the nortli of Roclie McLean, the western shore for a distance of
a little over a quarter of a mile, is occupied by a series of dark-gray
slaty rocks, the only .structural feature discernible being the planes of
cleavage, which dip northward at a high angle. This comes in contact
with, and is somewhat altered by, a small intrusion of diabase which is
doubtless an extension of the large mass which comes out on the
eastern shore at Quinn Point, To the north of this diabase, the mas-
sive breccia-conglomerate again outcrops, and is penetrated by a
mass or dyke of similar diabase, but with this slight interruption con-
tinues northward along the shore almost as far as Island Point.

This point is so named because of the existence at high-water of a
narrow and shallow channel separating it from the western shore. It
is composed of a iimch squeezed, contorted and altered slaty grey wacke,
continuing a considerable quantity of epidote. It is pierced through-
out by small and intricate granitic intrusion which have evidently assis-
ted matei-ially in hardening and otherwise changing. To the north this
rook is again succeeded by a conglomerate, containing the usual abund-
ance of granitic fragments embedded in a dark-green diabasic ordioritic
paste, resembling a diabase-tuli'. Aboutaquarter of amilenorth of Island
Point, this rock comes in contact with a fine-grained hornblende-granite
that forms the shores of the bay to the south of Pointe a la Barbe,
extending inland in a north-westerly direction and possibly connected
with the mass of granite exposed on the western shore of the lake above
the old Fort Narrows, although it is very different in appearance from
this.

In many places, this granite shows dark patches, generally oval or
rounded in outline, varying in diameter from a few inches to a foot or
more. These patches are caused by the segregation of the coloured
constituents and the more or less complete exclusion of the felspar and
quartz. They constitute what are familiarly known as the " dark
spots" (ausscheidungen) so commonly seen in granites, and evidently
represent the tirst-forraed nuclei in a slow-cuoling magma.

Quinn Point, is the name usually applied to a series of rugged
hills that form the shoreward extension of a pronounced range that
extends with little interruption for some miles to the north-east. The
rock composing these hills is a dark greenish-gray uralitic diabase, in
which the ophitic structure is generally apparent to the eye. The rock
varies in texture, the coarse phases assuming more of the holocrystalline
or granitoid structure, characteristic of gabbro. Jointed structure is
very perfectly developed, one set of planes dipping westward <; 80° while
another series dips eastward <^12°. The rock is composed chiefly of

■]

THE OTTAWA AND LAKE TEMISCAMING.

193 I

Cull Rock
rshincl.-.

pliigiocliise, which frequently contains much disseminated iron oxide,

<,'iving it a red hue, and hornblende, which has evidently resulted from

the alteration of augite. A small ijuantity of some carbonate (probably

dolomite) a little interstitial quartz and titanic iron ore were also
noticed.

The Gull Rock Islands are situated about half a mile nortii of Quinn
Point. There are two of them, presenting low rounded and well
glaciated surfaces, but little raised above the high-water level of the
lake and almost destitute of vegetation. The rock composing them is
the breccia-conglomerate, containing very numerous and often well
rounded pebbles and boulders, chiefly of red and reddish-gray granite,
with some of a compact dark-green altered diabase and a few of a fine-
grained greatly crushed quartzite. The matrix consists of the same
sort of material in a finer state, with greenish chlorite filling in the
smaller interspaces.

Moose Rock is the name applied to a huge boulder of rounded out- :mo()s(! Rock,
line, perched upon a shoal. It is almost thirty feet in diameter and
must have been detached from the cliffs of similar rock on the east
shore, over a mile to the northward of its present site, it has been
moved during the glacial period.

The northern end of Point a la Barbe, on the west shore, about two Hrnxi.i nf
iiiiies south of the Old Fort Narrows, is formed by an island which, at ]/,|l.'i',t/^ '^
high-water, is divided into two almost equal parts, connected by a
slender rocky peninsula. The rock composing it resembles the finer-
grained, harflened and altered matrix of the breccia-conglomerate. On
the opposite shoi'e a steep rocky point juts out into the lake, forming a
niUTOws. The breccia-conglomerate is here exposed for a considerable
distance along the shore either way, reaching to within about a quarter
of a mile of the mouth of the Little River. The shore-line at this point
rises steeply into a hill nearly four hundred feet in height, forming the
shoreward extension of a conspicuous ridge that runs for several miles
to the north-east, and marks the southern limit of the Little River
valley. The rock has a strike of about N. 00^ E., and a dip at low
angle, less that 5\ to the north-west. The breccia-conglomerate here
passes upward, by a gradual diminution of the larger fragments, into a
compact, fine-grained arkose sandstone or gieywacke, that is exposed
along the shore toward the mouth of the Little River. Under the Micioscoiiic
microscope, this rock is seen to be made up of partly rounded frag- charac -r.
ments of quartz, orthoclase, microcline and oligoclase, embedded in
a matrix proportionately less in quantity and composed chiefly of
chlorite and sericite. The fragments are nearly equal in size and show
13

■ ,^

;■■
.;.■:

■1"!

Mill:

ii:!k

0\-rlying
bciN,

Rocks near
Old Fort.

Granite area
nortli of Old
]''urt.

Cliaractcr of
granito.

194 I

NIPISSIN'(i AXD TKMISCAMING REGION.

no pronounced rounding. The greenish colour is owing mainly to the
large amount of chlorite present in the matrix.

To the north, and in ascending order, this rock is succeeded by a
somewhat coarse-grained sandstone or grit, which forms the point
immediately north of the mouth of the Little River. It also extends
across the lake*, occupying a corresponding promontory on the west
side, known as Blueberry Point. On both sides of the lake the rock
occurs in thick massive beds, the stratification being shown only by
the occurrence of conglomeritic bands disposed in a somewhat con-
stant direction. The rock is much jointed and broken, the fragments
having a rough "hombohedral outline. To the north, it is concealed in
great part by the deep and extensive sand and gravel deposits that
form the narrows opposite the Old Fort, but occasional outcrops may
nevertheless be noticed. The rock extends along the east shore of
the lake, nearly three quarters of a mile north-east of the Nar-
rows, where it reposes directly on a massive red biotite-granite,
although the actual junction is concealed. To the south of the nar-
rows, the rock occurs either in horizontal beds or dipping at a low
angle to the north-west, but north of the narrows it seems to dip
S. 35° E. < 20°

A specimen obtained from a point composed of this rock about half
a mile east of the Old Fort, is a pale yellowish-green coar.se-grained
quartzite or grit. The thin section under the microscope shows it to
be composed of quartz and felspar embedded in a groundmass made up
of pale yellowish-green sericite, for the most part present in exceed-
ingly minute scales.

The granite which replaces the quartzite to the north-east of the
narrows, is exposed on both sides of the lake. It forms the western
shore as far as Paradis Bay, a distance of about four miles, and
extends from half a mile to a mile inland. On the east side it com-
poses Wine Point and the southern shore of Kelly (Priests) Bay,
extending for a short distance west of the steamboat wharf to the
point already mentioned, about three-quarters of a mile north-east of
the Old Fort Narrows. In all, these granite exposures cover roughly
an area of six miles. Microscopically, the granite is rather coarse in
texture and of a deep flesh-red colour, owing to the marked predomin-
ance of the felspathic constituents, all of which have been abundantly
stained by iron.

Several small areas were noticed which have assumed a greenish
colour owing to the epidotization and sericitization of a portion of the
felspar ; but such decomposed portions are proportionally insigniticant,

•]

TflE OTTAAVA AND LAKE TP^MISCAMmO.

195 I

and the whole mass of the rock is extremely uniform, not only in colour
but ill the relative abundance and mode of development of its mineral
constituents. The (juartz occurs for the most part in somesvhat
rounded tliough itrejLfular isolated areas, giving to the rock aconglome-
ritic or purpliyritic appearance, a fact noted by Sir William Logan on
the manuscript map embracing his survey of this lake made in 1S4">.
Indeed, the rock at first glance presents a marked resemblance to some
of the brick-red (juartz-porphyrites of Lake Superior. The ferromagne-
sian constituent is present in very small quantity and is now almost
wholly converted to chlorite, the deep green colour of this mineral
being probably the reason that the rock has hitherto been described as
a hornblende-granite.

On previous geological maps covering this area, this granite received ronncr views
the colouration usually applied to an acid eruptive, and as nothing ^\^[^ granite
was stated to the contrary, it was very naturally inferred that, as such,
it was of later age than the Huronian elastics with which it is associ-
ated. Sir William Logan in his early report does not give any details
of its relations with the neighbouring stratified rocks, but only speaks
of it as "interrupting" the sandstones on Lake Temiscaraing. During
the progress of the present survey, a detailed examination was made of
the line of junction between this granite and the quartzite-grit. The
best locality for investigating the various contact phenomena, is situ-
ated in the small bay immediately west of the steam-boat wharf at
Bale des Peres. In addition to the observations made on the ground
a large suite of specimens was obtained illustrative of the line of junction,
for microscopic examination.

The facts obtained indicate the derivation of this quartzite-grit or Clantic rocks
arkose from the disintegration, i}i situ, of the granite, and is believed to jj
be an almost unique example of the recognition of a portion of the ori-
ginal granitic floor upon which the Huronian sediments were deposited
and from which they were derived.

In the vicinity of the line of junction between the two rocks, the Line of jimc-
arkose or quartzite may be poen dipping away from the mass of the '"""
granite at a very low angle. Tlie massive and jointed character of the
beds of the arkose, render it impossible to ascertain exactly all the
minute details of the structural relations, but it is clear that the quart-
zite originally transgressed upon the surface of the granite almost hori-
zontally. The granite has been unequally eroded and truncated, so
that the present line of contact between the two rocks is undulating
and irregular.
13^

■ .-4
I

■ -9

til

■■•; t

'■■An'

|;^il]

ill'

!--:i

I 1

196 I

NIPISSIXG AXD TEMISCAMIXG KKHIOX.

I fi-

s«

Cliiiractcr of
uiirtlti red
granity.

Microeliiit;
felspar.

Passagf 1m(].m. From a distance, the line appears to be sharp and abrupt, the green
ish colour of tlie quartzite showing up very clearly and distinctly in
contrast to tiie red colour of the granite. A closer inspection, however,
showed that there is a gradual passage upward and outward from the
main granite mass to the overlying arkose. Maci-oscopically this pas-
sage consists in a gradual loss of the red colouration of thn unaltered
granite cand the progressive appearance in its arkose of a yellowish-green
hue, although along the immediate contact there is no visible change
in the position of the constituent minerals.

Thin sections of the least altered portions of the granite exhibit a
normal holocrystailine hypidiomorphic structure, witii a tendency to
idioniorphic development on the part of the plagioclase. The rook is
a rather typical biotite-granite.

Tiie quartz is somewhat cracked and the felspar and biotite are more
or less altered, but the rock, as a whole, is fairly fresh, and neither
dynamic nor chemical forces have acted on it to such an extent as to
render its true character and origin doubtful.

The junctions between the grains of the various minerals are sharp
with no interstitial granulated material. The quartz is the ordinary
granitic variety and Is tilled with minute inclusions, frequently
arranged in irregular interlacing bands. ^lany of these, when liighly
magnified, prove to be cavities filled with fluids and often containing
movable bubbles. The larger quartz grains, under polarized light,
are seen to be made up of an aggregate of smaller grains with differing
orientation, and the quartz has a distinct but not excessive undulatory
extinction. The predominent felspar is generally microcliiie, which
can be seen in all its various stages of development from grains
exhibiting only an indistinct moirt^ structure (Plate V., fig. 2) to those
in which the cross hatching is perfectly developed (Plate V., fig 2.)
The foimer, however, are the more aVjundant. It is turbid and much
stained with iron oxide.

Plagioclaso. Plagioclase is as a rule quite abundant, and as already remarked,

exhibits a tendency to idioinorphic development. It is frequently
embedded or intergrown with the orthoclase and microcline. The
individual sections are broad and tabular, parallel to M., and show in
great perfection the fine striation due to multiple twining. Their
outlines are mote or less rounded. Carlsbad twins appear to be rare,
but were occasionally observed. Zonal structure was noticed in only a
very few instances and then was not at all pronounced. Like the
o.'thoclase and microcline, this felspar is turbid, in consequence of
incipient alteration, and little scales of sericite are scattered through

(ANlO«

]

THE OTl'AWA AND LAKE TKMISCAMINO.

197 I

it. Inclusions of biotite are not infrequent. Bending of the twin
lamella* is rare, and exists only in a very slight degree. The mean of
several determinations gave about -f 10° as the extinction-angle
measured on M., between adjacent lainellio, showing the felspar to
belong probably to the acidic end of the oligoclase series. As usual,
where alteration is commencing, it shows itself in the centre of the
crystals.

Biotite was the on' ' ferro-magnesian constituent noted in the sec- Biotite.
tion. It forms irregular plates and Hakes which are considerably
altered to chlorite. The original brown colour of the material has
been changed to a light-green, but without entirely obliterating the
optical characters of the biotite. Inclusions of ilmonite with leucoxene,
are common. Tlie mineral is not very abundant in this particular
section.

Ilmenite is the iron ore present in the rock, always accompaniec by llnunite.
its alteration-product leucoxene, and in some instances immediately
associated with zircon and apatite crystals. (Jcuasionally it may be
observed replacing titanite, skeleton forms of the latter mineral, with
sharply defined acute rhombic outlines, being filled with a mixture of
carbonates, ilmenite, etc.

Chlorite is present in the rock as the final stage of alteration of the Other constit-

1 ■ , ., Ufiit minerals,

biotite.

A few irregular grains and crystals of zircon with well-defined zonal
structure were noted, and exhibited the usual optical characters of the
species.

Apatite is also present, but is not very abundant, occurring in small
crystals and irregular grains.

Sericite, or an allied hydrous mica, is present in minute scales and
flakes scattered through the felspar, as the result of their alteration-
Red oxides of iron are abundant.

At the other extreme, the derived arkose or quartzite-grit show
distinctly rounded and water-worn fragments, chietly of grayish trans-
lucent .]uartz, varying in size from those only microscopically observ-
able, to others which are sometimes an inch in diameter and are arranged
in layers which have evidently resulted from a sorting of the material
by water action. These fragments are embedded in a groundmass or
cement varying greatly in proportionate quantity and composed of a
contused mass of minute sericite scales, being the argillaceous product
of the decomposing felspar.

Ilcrived
inatcrials of
till' arkose.

l.r.'

H |l

|tH

iji'

198 I

NIPISSIXG AND TKMISCAMING KK<iIOX.

Triitrnss of Tlie scries of thin septions studied represent the various stagH«i in tlie

(IcKiadatiun I'f ...11 1 . . . • . 1? 1 • 1 1

Kiaiiitt'. process 01 tlit; cieyradation ot the ^'ranite, 111 ooiiseiiuence or wliion ilie

overlyinj,' arko.^e lias l)eeii produced. Tlie lirst step shows tlie d(>velop-
inent of inicrorHiie at the expense of the orthochise, accompanied hy an
incijiient sericitization of the felspar-, which is notice ihle, to a con-
siileral)le exh^it, even in the least altered specimens. This is accou.-
panit d by marked alteration of tlie hioiite to chlorite, the develop-
ment of a distinct undulous extinction in the (juarlz, and a cracking
SicuimI stM, r of some of the individual grain-s. A further stage is reached when the
Huartz is accompanied by the occurrence of mosaic-like areas between
the larger grains, while these latti-r show very pi'onounced strain-
shadosvs. Tiio [il gioclase liktnvise shows more frci|atnt evidence of
presure in its tv/inning, the lamella' ot'ten in these cases ending
abruptly against cracks traversing the crystal, lending of the
lainellie is more frequent, while the alteration of biotite to chlorite is
more ct-Hiijilete, and is frequently accompanied l>y the ih!jiositit;n of
iron ore between the Hakes.

Third stagt'. This is closely followed, marking what may be Cilled the third step

in the transition, by an aj^preciable advance in the alteration of the
felspar, especially of the plagiodase, which becomes traversed by a
series of cracks HUed with sericite, the alteration exttnding outwani
into the main mass of the individual grains ; but there is still no evi-
dence of motion or shoving apart of the fragments.

Fourth .stai^(. A fourth, and somewhat sudden advance, appears when the
alteration of the felspars has proceeded to an extreme degree, while
certain fragments have been shoved aj)art. Kach individual grain
still oc 'ipies the same relative position with regard to the other mine-
ral constituents, but in places portions of quartz and felspar, especi illy
the former, can be noticed to have changed their position along certain
cracks traversing the grains, the portions, however, being never widely
separated. The plagioclase has been almost completely saussuritized,
lea\ing the unaltered quartz grains in almost the original position occu-
pied by them. The microcline and ortlioclase, though badly decom-
posed, hove not undergone such complete alteration as the plagioclase.

Fifth stage The fifth stage is reached when both ortlioclase and microcline have
undergone somewhat complete decomposition, some of the individuals
being now represented by an intricate mass of their alteration-proclucts.
This is accompanied by markedly uneven extinction in the quartz
grains, as well as by a cracking and separation of quartz and felspar-
crystals, which is more evident in the former.

Sixtli stage. The sixth and final stage in the process, shows, that the felspars have

almost entirely disappeared, although occasionally irregular cores o

i;koI.O(JI(AI, Sl'kvky ok Canapa

Vol. \.. Paht I., I'iat.: V

Fi(i. 1.

Fui. 3.

Via. 2.

Fig. 4.

Kui. 1.— Hiotitf-graiiite or granitite, iiciir Cf(]ar Point, cast side Ijakc Tfiniscaniing— orthoclase,
<Hiart/., jilagiodase and chloritizcd hiotitc. X •")-.

Ki(i. 2, — Effects of pressiire, graiudation, and tlie formation of niicrocline in arkose, near Baie dfs
PtTt's Lake TtMuiscaniing. X 52.

Fii;. 3.— Formation of niicrocline ar.d moving apait of minerals, of arkose resulting from degradation
of granitite, near Baie des Peres, Lake Temiscaming. X T)'.'.

I'll!. 4.— Deconi|K)»ition of felspar (niicrccline) in sit'i, forming arkose, near Baie des Peres, Lakc'
Teniisoaming. X 52.

Ma*

m >

t .;£!'

li.;;.

i'i

11; i»

■ARLC

('it

Stl :'

U: ^

1 ■ 1

( :

asajy,

In i^^BII

¥■'

■

tl..'

iiii'.

C'Ktl

eiiiit
Til.-

iietic

at'iiti
nu'iit

llfSS,

,1,'l'itS

ii clic
iiiici(

UllL'lli

has ol

the gi

T'lc
(.lis an
perpeti
diatel}
a consi
/ontal
a very
the ex]
near \
eastern
are coi
small J

This
seating
oceasio
hard, r
thieic a
weathe
of an ii
the exj

■J

rUK OTTAWA AND f.AKK TRMIHCAMINfi.

199 I

tho unaltered ininenil remain. Tlie ji^rmindiiinHs is now seen to consist
(if a line-gruincfl .scrioitic material, in wliich are embedded wliaiply
angular or sub-angular fragments with very pronounced uadulous
extinction. Tlio whole appearance of tho rock, both in the hand spe-
cimen and under the microscope, is that of a typical clastic (arkose).
TluTO is every evidence, how(>ver, that much of tho material has not
undergone any very wide separation, while the quartz fragments still
preserve a tolerably sharp outline, showing no pronounced water-
action.

The suite of .specimens obtained, exhil)its a still further stage, repre- INrcchaiucally
senting the whole process leading to a tliiai assortment and rc-arrange- \^.l[n\_
nicnt of the degi-aded material by w.ator into bands of diflering coarse-
ness, and resulting uttimaiely in tho formation of .somewhat typical
grits and conglomerates. The change has evidently been iirst mainly
a chemical one, primarily attacking the biotite, then the plagiocla.se,
niicrocline and orthocla.se and leaving the quartz alone comparatively
unchanged. The rock thus softened and loosened by decoiujiosition,
liasoflered a less elfectual resistance to the process of disintegration, the
process ending finally in the complete breaking down of the surface of
the granite mass and the formation of the overlying aikose.

The latter rock forms the western shore of the lake between Para- i,i,.,ni>li
dis and Martineau bays, opposite Bry.son Island, where it constitutes 'I'l'Htzitf.
perpendicular cliffs that rise from 150 to 200 feet, while the hills imme-
diately behind, continue with a more gradual upward slope representing
a considerable additional elevation. The rock occurs in almo.st hori-
zontal beds, striking with the lake, the structure .seemingly representing
a very shallow and narrow syncline ; the })eds near the southern part of
the exposure in the vicinity of Paradis Day dipping west, while those
near INIartineau Bay dip east or toward the lake. Almost the entire
eastern shore of the lake, as well as Chief, Drunken and Bryson islands
are composed of this greenish quartzite or arkose, excepting only some
small patches and strips of Silurian limestone, elsewhere described.

This greenish quartzite is remarkabl}' homogeneous, generally pre- its character
senting the characters of a coarse quartzose sandstone or grit, but
occasionally, as on Drunken Island, becoming liner-grained. It is very
hard, resisting well the general influences of weather, and occurs in
thick and much jointed beds, generally of a pale yellowish-green colour,
w(>athering in some cases to a light-brown to a depth of about an eighth
of an inch. It sometimes has a brownish-green colour, in which case
the exposed surfaces gradually assume a yellowish-green colour, and in

M ■'

fi'lil

il!^

200 I

NIPISSINO AND TEMISCAMINO UKdION.

lifllM"

Rt-lntioiiH cif
prrcn <nmrt/.-

occHsiunivl oxposuros it, has a Iij,'ht-;4rayi.sh tint with irregularly dispo-
sod spots or areas of a greenish colour.

In the vicinity of the narrows bntween the eastern shore and Mryson
Island, the rock dips N. 22" W. < 3°, and for the most part runs in
low broad undulations. At a point on the east shore about one mile
and a (|uarter south of Wright's mine, this rock is seen directly super-
imposed upon the huminocky surface of a very massive breccia-conglo-
nierate. The letter holils the usual pebbles of eruptive material,
chiefly granite and diabase, and thechloritic matrix is very subordinate
in quantity. The e.xposure presents a well rounded and glaciated out-
line sloping at an angle of nearly GO' to the north. At the sunnnit,
about forty feet al)ove the water, the greenish cjuartzite seems to rest
directl}' upon the c mglomerate, presenting none af the usual transi-
tional slaty or greywacke beds. The beds of cjuartzite seem to run in
a somewhat undulating though approximately horizcmtal mannen
apparently conforming with the line of outcrop of the conglomerate.

Section iifiii

Wright'.s

mine.

About three-(iuartprs of a mile north of Wright's mine, on the same
shore, there is a \ery interesting section. Showing the usual breccia-
conglomerate at the base, very massive, and giving little or no struc-
tural detail. In ascending, however, it passes into a breccia, somewhat
similar in colour and comi)Osition, but in which the lines of stratifica-
tion can be readily distinguished. This is in turn succeeded by a fine-
gruintd, brownish, well banded greywackt' slate, some portions of
which cleave readily parallel to the bedding. This C(jntains i?'ome
smaller intercalat^ed bands of the breccia, in which dinbase and quartz
fragments prevail. This is in turn overlain by another bed of con-
glomerate thiit passes upwaid into the yellowish green (juaitzite-grit.
The dip of these strata is to the north-west, at an angle of 10, and the
whole thickness of the section exposed is about AO feet. The point
immediately south and west of Wright's mine is likewise composed of
the breccia-conglomei'ate, tilled with pebbles of eruptive material, and
the lode itself is situated in a similar though finer rock. In many
instances the chloritic matrix is seen to wrap or tlow around the en-
closed fragments.

West shoif, From Martineau Bay northward, for about two and a half miles,

dnt^iuB' • ' ^^^^ western shore is composed of a dark -greenish or greenish-gray,
medium textured diabase. For nearly the whole of this distance this
rock rises into clifls, sometimes 200 feet high. The mass of the rock
is much jointed and broken, and some of the jointage planes traverse
it for considerable distances, thus simulating the basaltic stiucture so
frequently assumed by similar basic eruptive masses. Under the

iL.t '' '

]

THE OTTAWA AND LAKE TKMISC^AMINO.

201 I

(liillwxe lllilN.i.

microscope thin rock is seen to possess a typical diabasic or ophitic Micnwcopic
structure, the interlacing idioinorphic laths of plagioclase penetrating ,i;;ii,.i„
the allotriomorphic individuals of nugite. The plagioclase has been
rendered more or less turbid by the development of the usual saus-
surtic products of decomposition, but many individuals still retain their
clear and limpid character. The augite has, however, been altered to
hornblande, the alteration being first to the fibrous form (the
more abundantly repiesented), and then into the compact green
trichroic variety, which is occasionally present. In some cases decom-
position has proceeded so far that chlorite has resulted. A small
quantity of unstriated felspar in Inroad, irregular areas, that may be
orthoclase, was noticed, while a considerable (juantity of (juartz fills in
the interspaces. Occasional Hakes and scales of brown biotite are like-
wise present, at times altered to chlorite. The ilmenite is almost en-
tirely altered to leucoxene, a'.t' nugh undecomposed portions remain.
This diabase constitutes the VI „ical clilFs known as the Manitou or Kxtcnt of
Devils Rock, forming the shoreward e.xtension of a huge mass that
occupies the intervening area between Lake Temiscaming and the
Montreal River, and which, extending across this river, forms a con-
siderable strip on its south-west side. It also composes the area to the
north-west, extending to the shores of Portage Bay, on Ray Lake, and
lieyond.

To the north of this diabase, on Lake Temiscaming, the characteristic
breccia-conglomerate again conies in. The finer portions of the matrix
are composed of a much hardened chlorite-slate or greywackt', while
coarse-grained varieties resemble in appearance a diabase tuff. The
pebbles are usually abundant, and some of these resemble the diabase
with which this rock is associated. Other pebbles are of (juartz, and
some are of a dark-gray compact felsite or greywackt', while a few
consist of a pale-yellowish, line-graim-d hiilleflinta-like rock. Near a
clearing on the west shore, a little south of Peroy Island, the rock ex-
hibits a similar line-grained chloritic groundmass, containing very
numerous small fragments, chiefly of felspar, while the rock itself as a
whole greatly resembles a chloritized tuti' or trap ash.

This is succeeded to the north (and doubtless in ascending ordei-) by
a fine greenish compact slaty greywacke, exposed in the vicinity of
Farr Creek, that continues beyond Lawlor's farm. For about two
miles in the vicinity of Haileybury, the western shore is occupied by
Silurian strata. About two miles north of Haileyburj', the basal bed
of the Silurian consisting of a coarse grit or conglomerate, rests uncon-
formably on the raammillated surface of the compact green slate of the
Huronian.

ti'ii

Further ex-

IKISIIM'S of

tiri'fciiicoii-
i^loiiifiati'.

t • !

Sliity pii'.v-

i I

. .i I

; ' s

,; ' •

, « ^ ■

] !

■! ;■' r;;

Rocks of
Wal)iH liny.

Pyrittjus ooi;
glomerate.

Exposure on
Sutton Jkiy.

' I

202 I

XIPISSING AND TKMISCAMING HKGION.

This slaty I'oek, near the junction between tiie two formations, is
very much hardened and presents alternating bands of greenish and
brownish colours, so frequently characteristic of the middle member of
the Huronian of the distinct, and thetie bands have a general direction
of iS. 70' W. The siiore-line where the rock outcrops, is more irregular
tlrvn that to the north or south, with two small olf-lyiiig islets About
a mile north of the contact, the slate passes into the breccia -conglomer-
ate, containing man}' pebbles and boulders of grayish slate, compact
quartzose and halleilinta-like rocks, and pebbles of diabase of varying
dc;grees of texture. The matrix in which these fragments are embedded
is, as usual, dark-green in colour, while the whole mass of the ruck
presents little or no evidence of stratification. In ^eneral, however,
it may be stated, with some degree of confidence, that the structure
exhibited on the shore from the contact to the south as far as the dia-
ba.se mass, is that of a shallow syiicline, the breccia-conglomerate form-
ing the basal beds with ihe slales superimposed without bie.ik.

Where the fragments are almndant in the conglomerate, tin fo is fre-
quently present a considerable amount of pyrite, which in .'•ome cases
acts as a sort of cement, inclosing these fragments. The oxitlation of
this jiyrite and its subsecjuent removal, has left a series of rusty cavi-
ties that are rather characteristic of these outcrops.

The last exposure that may be mentioned here, is one of the breccia-
conglomerate which occurs on the north-east shore of Sutton JSay,
forming hills that ivre rather conspicuous and rise from a somewhat
extensive marshy Hat. The rock presents the usual dark-green chlorite
groundmass. This matrix encloses larger j)ebbles of red and gray
granite, green diabase of sc^veial varieties and degrees of coarseness,
and some fine-grained compact greywackc-slato, with a few of gray
quartz. The larger fragments, especially those of granite, possess more
or !es. rounded outline, while most of the smaller fragments, and
especially those representing basic eruptive material, are decidedly
shfirp .ind angular. The rock is massive and for the most part
structureless, but planes that possibly represent the original bedding
dip N. W. < 25\

RivKPv AND Lac ues Quinze.

Tlivur (Ic-i
tiuiuzo.

The River des Quinze, doubtless received its name from the fact that
fifteen portages have to be made between Lake Temiscamiiig and Lac
des (Juinze, but this numl)er may bo diminished under some circum-
stances. Although the stream presents considerable stretches of deep
water with little or nt) current, it is, as a whole, wild and turbulent.

■]

RIVER AND LAC DES QUIXZE.

203 I

The river has a general east-and-west cUrectiun, aud in a straight line
is .'.bout thirteen miles long, although this distance is incieased to
eighteen miles by means of tlexuies. It enters the north-eastein
corner of Lake Temiscaming in a shallow indentation known as Paul-
son ]5ay. With the Blanche, which reaches the lake a little over a ConfUunce
mile fuitlu.'r west, it forms a delta with low marshy islands, and only lihuuiu..
two channels can bo utilized for purposes of navigation. The mon;
easterly of these two channels is seldom used, on account of its being
extremely shallow, while the western or main channel is of good depth.
About half a mile from the lake, a rather narrow and crooked, though
deep and navigable channel joins the (^uinze, with the main portion of
the Dlanche. This is known as the Chenal du Diable, and during
freshets the waters of the Blanche follow this channel to the lake, but
during the summer months the current in this channel is reversed, and
a considerable portion of the waters of the C^uinze reach the lake 1 1}-
this somewhat circuitous route.

The Biver des Quinze is generally a little over a mile wide. The banks, wi.ith and
especially on the north-west side, are low and liable to inundation, ^''-''-^^tt'''-
The .south-east bank is somewhat higher at ]\Iiller Point, with a hill of
gravel and boulders.

In ascending the river, the fust rock-expo!.-iure is on some small islets AsrcndiiiK
nearly opposite the North Temiscaming P. O. (McBride's). The ti,,. liviT.
rock is the breccia-conglomerate of the Huronian, the matrix being a
very compact, fine-grained material of dark green colour, through which
are disseunnated occasional pebbles as well as angular fragments of a
jirayish granitic rock. There is little or no evidence of stratification.
The further ascent of the river exhibits a corresponding rise in the
geological .scale. The first three lapidt^ come very close together, and Raiiids.
are not more than a mile in all. The first and second rapids each show
a descent of about twelve feet. The third has a fall of about sixty
feet, and is one of the worst on the river. Tlie rock exposed at the
several portages, is a dark-gray micaceous slate, tiie cleavage or foliation
planes, which are the only distinct structure exhibited, showing abund-
ant small black scales of biotite.

Theie are many lighter coloured streaks running through vlie Rucks
rock, more or less parallel with one another, which seem to be com- ' "^
posed mainly of felspar and quartz. These occur in irregular curving
and often branching and lenticular areas giving a decided foliation to
the rock. They do not appear to represent coarser and more tjuartzose
l.'ands of the darker coloured slates with which they are associated, but
are more or less veinlike in structure and secondary in their origin.

I'll

' !'.'■

! ! li I

,',e; .. .

'11
ii

^flfp

■;. 'il

I, ?;

! I

Fourth rii|iiil

basi'.

iiiul (lia

Alti'iation of
tlio iliiibase.

204 I

NIPIiSSING AND TKMISCAMING KEGION.

The strike and dip could not be ascertained with any degree of certainty,
but the rock, from its lithological character and apparent stratigraphical
position, represents the lower portion of the slate, or middle member of
the Huronian, overlying the breccia-conglomerate noticed as occurring
near the mouth of the river.

xYbove this third portage, there is an interval of three miles of deep
unobstructed navigation, to the fourth rapid, immediately above the
mouth of Tiger Creek, an important tributary coining in from the north
side. The river is here divided into several channels by rocky islands,
the largest of which, Burnt Island, is nearly one and a half miles in
length. The main channel which runs to the north of this, is one long
succession of heavy rapids with a total fall of about eighty feet. Tlie
portage-route, fibout two miles long, follows the north bank.

On this portage, the rocks met with are dark greenish-gray slate, much
cleaved and jointed and probably dipping to the south-east. In places
they show considerable alteration and development of sericite, the alter-
ation being greatest near the eastern end of the portage. These slates
continue to the upper end of the island, where they are interrupted by
a mass of uraltic diabase and ani})hibolite, about thvue and a half miles
in breath, which extends southward, and is probably continuous with
similar rocks exposed in the north-east corner of the township of
Duhainel and the eastern portion of the township of Guigues. This
rock is often massive, but not without traces of foliation and towards
the eastern limit it passes into a distinct grayish-groen amphibolite, in
which considerable mica has been developed. Under the microscope,
it is found to be composed chiefly of plagioclase and hornblende, and
thus to be classed with the diorites, but it evidently was originally a
diabase, as a well mai'ked ophitic structure is still apparent. The augite,
originally present, is almost wliolly converted into hornblende, while
during this process of uraliti/atiou, as is usual, a considerable quantity
of epidote has been developed. It is a straw-yellow colour, exhibits
strong pleochroism, and has often faii-ly good crystallographic outlines,
although occurring mostly in irregular grains and patches, associated
chielly with the hornblende.

The process of uralitization is here very interesting. The augite
alters first into a compact green trichroic hornblende. Where it has
suffered most from dynamic action, a fibrous variety of hornblende
(actinolite) has resulted, which has in turn decomposed into chlorite
that still preserves much of the pleochroism of the hornblende. Between
crossed nicols, the matted aggregates of scales of chlorite show collect-
ively the deep-blue polarization-colour so often exhibited by it. Much

■ARLOW

]

RIVEU AND LAC DES QUINZE.

205

of the plagioclase is remarkably fresh for such a decomposed rock, but
a great deal of it shows a soinewliat advanced saussuritization, the
resulting epidote, zoisite and serioite being especially abundantly
developed where the rock has been most sijueezed. Ilmenite occurs in
aggregates of small grains which are each surrounded by a rim of
leucoxene. Quartz, although present, is not at all abundant. Where
pressure has been greatest the rook passes into a typical hornblciule-
schist or amj)hibolite. The ophitic structure cannot be detected under
the microscope, while pressure has caused the breaking up of the original
bisilicate individuals, so that they are now represented by many small
shreds and fragments, arranged with a more or less parallel alignment.
A groat deal of epidote has been developed, while the ilmenite originally
present has been almost converted into a brownish sphene, now seen
in irregular grains or aggregates of grains scattered through the rock.
Associated with and apparently caught up in this eruptive are certain,
small patches of sericitic and epidotic slates, while on one portage (the
tenth from Lake Temiscaming) an interlamination of light- and dark-
grjiy (juartzite with red jasper and magnetic iron ore occurs, the whole
running parallel with the foliation of the inclosed rock, N. 20^ E., and
dipphig N. 70° W. < 70'.

Above Burnt Island, the seventh portage, from the lake, is
merely a lift over a rocky islet to avoid a small rapid in the river.
A short distance further up, the next or eighth portage is reached.
Tliis is but a short carry across to a small lake, to the north-east of
the river and a short paddle across this brings us to the outlet at its east
end. Another short portage along the bed of this outlet comes out again
to the main stream. Above this is a sharp turn in the river, its direc-
tion changing abruptly to a south-easterly bearing. The canoe-route
again leaves the main stream below thi^ elbow, a very rough portage
on the southeast side, leading to a narrow lake about half a mile in
length. The next portage, divided into two carrys by an interven-
ing pond, counts as the eleventh and twelfth, leading back to the main
rivei'. The route thus follows a narrow valley running parallel to the
river, avoiding a very rapid stretch of river, with a total fall of about
fifty feet. The direction of the river here coincides with the foliation
of the hornblende-schists. The thirteenth portage is on the east side of
the stream, and is sometimes called Cypress Portage. It is over half
a mile in length, and is occasioned by a rapiil with a fall of osiw twenty
feet.

.•^(•vcntli to

thirti'cntli

l«atiigc.

Toward the head of Cypress portage, the uralitic diabase, largely |)i,(i,,,j„, ,,t
changed into a rather typical hornblende-schist, is penetrated l)y small <'y|'i»>s« I'ort-

f«lr"

!?»■

H'l

is§

206 I

NIPISSING A\D TEMISCAMING REGION,

At Miiples
jiDrtage.

Contact with
gneisses.

Character of
gneiss.

i'
«■

. i-

stringers composed chiefly of flesh-red felspar and gray (juartz, with
occasional small fragments of hornblende. The connection of these
small apophyses of granitic material with the lai-ger parent mass of
hornblciide-granite-gneiss exposed further east, was clearly established,
and these lenticular patches of quartzo-felspathic material become moi'e
abundant as the vicinity of the granite-gneiss is approached. The lock
contains considerable secondary biotite, developed chiefly along the
planes of shearing, and this, in conjunction with lighter fclspathic
bands produces a very distinctly foliated rock. The foliation dips
westwards at a high angle, generally about 50°.

The same rock continues, with the interfoliation of lighter and darker
bands, across the fourteenth or Maples portage, at the head of which
the course of the river turns rather abruptly to an easterly direction
while the width is increased to a quarter of a mile. The dividing line
between the hornblende-schists-gneisses crosses this lake-like expansion
obliquely. Although the actual contact is not exposed, the two rocks
are seen within a very short distance of one another, both striking
toward the north-west, while the dip of the foliation is to the south-
west at an angle of about 50°. Tlio junction between the two is
evidently one of intrusion, the granite-gneiss piercing the amphibolite
in the form of the small interfoliated pegmatite-like streaks and
patches above described, and it appears that the irruption of the horn-
blende-granite-gneiss was the cause of the foliation and alteration of
inceptive diabase, producing the hornblende-schist.

The granite-gneiss just alluded to, is a reddish, very distinctly foli-
ated rock, the foliation being determined by the more or less parallel dis-
position of the fragments and individuals of hornblende. The thin
section shows the rock to be composed essentially of orthoclase, niicro-
cline, hornblende and quartz, with sphene, epidote, zircon and apatite
as accessory or accidental constituents. Much of the orthoclase occurs
as irregularly shaped individuals or phenocrysts embedded in a iiner-
grained mosaic composed of broken up fragments of felspar and quartz.
These smaller fragments very often assume the niicrocline habit, which
is evidently the result of prevSsure. The larger orthoclase individuals
show considerable alteration, especially in their central portions, and
although in some cases they exhibit tolerably sharp and perfect
crystalline outlines, they are usually more or less jagged, owing
to the breaking up of their borders to form part of the tiner-grained
mosaic. The hornblende is dark-green, trichroic, and occurs in irregular
shreds and fragn\ents having a marked {)arallelism. The sphene id deep
brown in colour, and occurs in characteristic wedge-shaped crystals.

•J

RIVKR AND LAC DKS QUINZE.

•207 I

Uocks near
the lake.

The epidole is evidently of secondary origin, and is present in irregular
grains and masses of a deej:) straw-yellow colour and strong pleo-
chroism. Zircon and a[)atite are in small acicular prismatic crystals.
The reddish colour is imparted by the presence of iron-oxide, which
fills the cleavage-cracks of the felspar as well as the minute fissures
present in the rock itself.

This rock continues as far as Lac des Quinze, but near the lake it
becomes coarser in textun^ and more highly porphj^ritic, the reddish
crystals of orthoclase being frequently as much as half an inch in
diameter. The foliation is rather obscure, but on the lake itself is
more evident.

The fall overcome by the last or fifteenth portage before reaching
the lake is about ten feet.

Lac des Quinze takes its name from the river The general summer L;ic des
level of this lake, as determined by the mean of a large number of '''""'"' •
aneroid readings, is 848 feet above sea-level. The area of the lake is
approximately forty square miles. A considerable portion of the
northern part of the lake is, however, not represented on the accom-
panying map. There is a Hudson's Bay trading post on the lake, known
as Long Point, while lumbermen now at work in the country near
Lake Winnowaia or Expanse, a little to the east of the present map-
sheet, have several farms or clearances, and depdts for supplies.

The main body of the lake extends to the south-east from the outlet Form andout-
for a distance of about eight miles, with an average width of a little """"
over a mile. A second, generally about a mile wide, runs northward
for a like distance from the outlet and then divides into two bays,
which continue with the same general direction for about three miles
further, the more westerly of the bays being the one followed in going
to Lake Abitibi. About two miles to the east of the north arm, a
second narrow inlet extends to the north for about three miles. From
the south-eastern extremity of the main body of the lake, two arms
branch oflf. The larger one runs to the north-east for about fifteen
miles, gradually tapering to a point, where it receives the Upper
Ottawa. The second arm runs to the southward for about five miles,
and at its south-easterly corner reaches the western terminus of the
road from Bale des Peres. A new road from Lake Temiscaming to
Lac des Quinze, to the north of the River des Quinze, starts from the foot
of the first rapids, but is not yet completed.

The .several arms of the lake have all been eroded in a direction corres- Surrounding
ponding with that of the foliation of the gneissic rocks, and evidently '""'^^'^*'-

!' i

-■n'l

208 I

NIPISSINO AND TEMISCAMING REGION.

represent the more schistose and least resistinj^ belts of these rocks. The
prevailin;^ rocks are gray granitic and dioritic-gneissea, the latter
containing usually a considerable proportion of biotite in addition to
the hornblendu, and with an increase in the abundance of the bisili-
cates, passing into an almost black, glistening amphibolite, in which the
schistosity is always well marked. Quartz is present in considerable
quantity, particularly in certain bands, and epidote was also noticed
as a somewhat abundant constituent. At several points on the lake
massive crystalline diorite was observed. The gneisses liavo a well
marked foliated structure, the inclination of this foliation varying from
30° < 45 in a westerly or north-westerly direction.

■

) ■•;

■'1

^^^H^B

f J-

i^^H m.

'.V.

'HI

■>

'i|l^

Kctjjawa.

Fiirmanrl sizn

p]l»'vati<>n.

Lake Keepawa.

The name Keepawa or Kippewa means, freely translated, " a
very narrow passage between steep rocks," and I'efers to the presence
of a gorge in the northern part of the lake, now generally known as
The " Canal." The lake is very irregular in form and full of islands.
In general the lake may be described as filling several valleys
approximately parallel tc that occupied by the southern portion of
Lake Temiscaming. The general trend of these valleys, like that of
Temiscaming, cuts across that of the foliation of the gneissic rocks,
except in those portions to the south-east of Roche a Corbeau and the
Beauvais Narrows, where the main direction of the lake corresponds
rather closely with the foliation of the adjacent gneisses. The greatest
length of the lake, from Chemagan Bay on the north, to the portage
leading out of Jeanbeau Bay on the south, is almost thirty-two miles,
on a line bearing S. 12° E. It may be said to be divided into two
main portions occupying an approximately parallel position, each, how-
ever, branching off in bays and arms in various directions. These two
larger portions are connected about the centre by a few comparatively
narrow channels. The portion to the south-west, extending from the
outlet at the north-west end of Sandy Portage I>ay to Jeanbeau Bay,
measures twenty-seven miles in a direction of S. 38° E. ; while the
large body of water to the north-east, reaching from the north-west
end of Taggart Bay to the outlet of Hunter Lake, a distance of twenty-
eight miles, has a general trend of S. 42° E. The ai'ea of Lake Keep-
av. . , 'ling the islands, is nearly 120 square miles. Its height
;'' a i'jvel varies from 87G to 88G feet. The Keepawa River, its

11 !• 1 o',.?k't, is a crooked and rapid stream which enters Lake
Temiscaiiiing a iutle over six miles below the Montreal River. The
lumbermen ha ve, however, built a dam across the Keepawa at the

■]

LAKE KEEPAWA.

209 I

north-west end of Sandy Portage Bay, thus raising the water-level. Artificial
The rocky obstructions between the south-western part of Lake Keep-
awa and the ponds at the head-waters of Gordon Creek having been
removed, a large portion of the Keepawa waters now discharge by this
artificial channel. In this way the " drive " for logs is much short-
ened and the water held back till required.

The greater part of the shore-line of the lake is somewhat Surrounding
high and rocky, the sui'face being often strewn with large boulders,
chiefly of the underlying gueissic rocks.

There is little level land, although clearances have been made and
farms cultivated in connection with lumbering. Most of the white
pine of first quality has been cut, but the shores are still beautifully
wooded.

Of the very numerous islands, McKenzie and Karl islands are the Islands,
laigest, the former being a little over five miles in length and averaging
about two miles in breadth, while the latter is scarcely half this size,
measuring a little over two miles in length by about a mile and a-half
in width.

The " Canal," already mentioned as giving its name to the lake, is a
picturesque feature, being a narrow gorge about a ([uarter of a mile
long with perpendicular walls of gneiss situated, about a inile north-
west of Mackenzie Island, and it leads into a couple of small lakelets or
expansions.

The rocks so abundantly exposed along the shores and islands of ( Jneiss of uni-
Lake Keepawa are remarkably uniform in composition and macro- tg,'."'
scopical characters. They are typical examples of " gneisses " being,
as a rule, very distinctly and evenly foliated, and exhibiting darker
and lighter-coloured bands of more or less basic character. The
more acid bands are usually of grayish, reddish, gray or flesh-red
colour ; while the more basic bands are of varying shades of darker
gray, becoming almost black in certain instances. The lighter-coloured
pliases are, perhaps, the most abundantly represented, and besides
occurring as interfoliated bands associated with more basic material,
these in themselves constitute the greater portion of somewhat impor-
tant and extensive rock-masses. Under the microscope, they are seen Microscopic
to contain orthoclase as the prevailing felspathic constituent, and
biotite as the principal and often the only ferromagnesian mineral.
They must, therefore, be referred to as biotite-granite or granitite-
gneiss. Besides these, microcline is usually abundant, together with
some plagioclase (usually oligoclase). A large amount of quartz like-
U

ill 1

struoture.

PJi ill

The darker
rocks.

Rocks near

Kippawa

post-oHice.

On sotithern
part of lake.

210 I

NIPISSINO AND TEMI8CAMIXG REGION.

wise accompanies the felspar. The biotite is, as a rule, fresh and of a
deep brown colour, occasionally showing alteration to chlorite
A little muscovite (most of which is of secondary origin), sometimes
occurs, but not in sufficient (juantity to characterize the rock. Besides
these, smaller quantities of epidote, sphene, sericite, chlorite, apatite,
zircon, magnetite, and sometimes allanite, are usually present.

Occasionally, somewhat darker and more basic portions are seen to
contain a compact dark-green trichroic hornblende in addition to the
biotite, the rock thus becoming a hornblende-granitite-gneiss. These
portions are usually of a dark-gray colour, and show a very n;arked
abundance of the coloured constituents.

The very dark-gray, almost black varieties, in which but little of
the lighter-coloured minerals can be macroscopically detected, often
show plagioclase as the prevailing felspar, while biotite is replaced by
hornblende, the principal ferromagnesian mineral, although biotite is
likewise almost invariably present. The constituent minerals are
essentially the same as those present in the more acidic phases,
differing only in their relative proportions.

The structural relations of these rocks show that they form integral
and inseparable portions of one complex, produced by differentiation
during the slow cooling of a magma of moie or less heterogeneous com-
position.

At the head of Gordon Creek, and in the vicinity of Kippawa post-
office (formerly Norclifl'e), the gneiss is very distinctly foliated, the strike
being about S. 55° E., the dip S.W. < 10° to 20°. The thick massive
bands in the high bluff to the north of the railway terminus, repre-
senting the more acid portions of the rock, are granitic both in appear-
ance and composition. Felspais, both reddish and grayish, are present
as well as quartz, and a very sparing quantity of mica. The quartz,
besides being present in grains and areas distributed throughout the
rock, also occurs as veins and masses, evidently representing the most
acid form of the prevailing pegmatite.

On the north-east shore of the largest island of the group, situated
about a mile east of Kippawa post-office, are good exposures of light-gray
and pinkish-gray quartzo-felspatliic gneiss, alternating with darker bands
which contain hornblende in addition to the more usual biotite. The
strike is east-and-west, with dip to the south < 35° to 45°. Along
the shore the basic bands have been weathered out more easily than
the acid ones.

Further to the south-east, toward Jeanbeau Bay, the gneiss varies
in strike from S. 50° E. to S. 60° E. with a dip to the north-east

BARLOW

]

LAKE KEEPAWA.

211 I

< 20° to 30'. North of Gordon Creek, the foliation of the gneiss
corresponds rather closely with the trend of the shore-line, dipping to
the north-east at varying angles. At Ureenorton Bay the schistose
gneiss is very basic and contains hornblende in addition to the
biotite. This rock also holds garnets and vein like bands of smoky
quartz. At the font of Gibson Bay, the gneiss is of the common
light-grayish granitite variety. On the south shore of Bryson Island,
there ar*> good exposures of a light-gray granititegneiss, the foliation
being much contorted.

Beavais Narrows cuts the foliation of the gneiss at a considerable North of
angle, the strike being S. 65'^ E. with dip to the north-east < 15° js'arrows.
to 2.5". On the south shore of Smith Ba}-, exposures of hornblende-
granitite-gneiss show the constituent felspar much decomposed and
a large part of the biotite altered to chlorite. At Fowler Point,
a knoll rising about forty feet above the surface of the lake is com-
posed of a fine-grained almost black quartz-mica-diorite. This
rock contains irregular patches and stripes of a much more acidic
gneiss, light llesh-red in colom", which .seems to contain felspar,
quartz, biotite and garnet, with occasionally some muscovite and
epidote. Near Edward's depot, on the north shore of Smith Bay,
the granitite-gneiss is as a rule very acidic, containing only small
quantities of biotite. At Somerville Point, the gneiss is a reddish
granitite much weathered and showing what appeared to be a very p^^•^^^
local strike of N. 40 E. The south-west shore of the lake opposite
Sunnyside post-office is composed of i-eddish granitite-gneiss, generally
striking with the trend of the shore, but sometimes showing many
local twistings. At Turtle Portage, the usual granitite-gneiss shows
a beautiful curve in the foliation, the strike gradually turning from
N. 80" E. to S. CO' E., with a prevailing southerly dip. At Hunter
Lodge Narrows and on Hunter Lake the gneiss strikes about S.
60' E., dipping in a southerly direction.

Along the south .shore of jNIcLaren Bay, the gneiss is usually of a Gneiss of
light-gray colour, rather fine-grained, micaceous and granitic in |j,^y '"®"
appearance, being tinged with iron-oxide. It usually shows a distinct
though imperfect foliation on account of the comparative scarcity of
bisilicate material. The strike is N. 82" E. and the dip to the south.
Microscopically, this is a typical holo-crystalline granitic rock or
granitite-gneiss, consisting essentially of orthoclase, quartz and biotite,
with apatite-zircon, sphene, a very little magnetite, much microcline
and some plagioclase, (oligoclase) small quantities of secondary musco-
vite and epidote are also present.

14^

At Somerville

ill..:

'! V !

:: :i

.11

' R

V m

:! *l

£xi>o«urea
near McKen-
zie iHliind.

Gneiss at
Campbell
Bay.

On Karl
Island.

m^i

Porphyritic
diiirite.

212 I

NIPI8SIN<; AND TEMI8CAMINO KEGIOX.

At the south end of an island immediately east of McKenzie Island,
there are exposures of the ordinary llesh-red granitite-gneiss. On the
north-west shore of McKenzie Island, the hornblende-granitite-gneiss
seems to change in strike from N. 20° E. to N. 50' E., thus conform-
ing with the trend of the shore-line, while the dip is to the south-east
at varying angles generally about 00\ At one point a vein of (juartz
(pegmatite) varyiiig in width from six inches to two feet cuts the
gneiss, of which it contains fragments. The gneiss here is well
foliated and often locally twisted. The gneiss composing the cliffs on
either side of the "Canal," contains a considerable quantity of quartz
and is much weathered and stained. It has a strike of N. 65^ E, with
southerly dip < 80'. At the south end of Campbell Bay, the strike
of the gneiss is north G2° east. A thin section of a specimen obtained
from the western shore, about two miles south of the entrance, repre-
senting the most basic bands, showed the rock to be a quartz-mica-
diorite-gneiss. The rock is nearly Vjlack, very evenly and distinctly
foliated and exhibits glistening cleavage-surfaces along the planes of
foliation. Exceptional bands are of light pinkish-gray colour, felspar
being the predominant constituent. Microscopically, this rock is
composed of plagioclase, orthoclase, microcline, quartz, hornblende
and biotite, with epidote, sphene, apatite, zircon and some pyrite, more
or less altered to limonite.

On the west shore of Karl Island, as well as on the island lying to
the south-west, the gneiss shows the usual variation from grayish to
reddish, with interfoliated darker bands in which the biotite is more
abundant. The strikes vary from N. 64' E. to N, 67° E., with dip to
the south < 60° to 70°.

xVt one place on the north shore of the lake, half a mile north of
the north-east point of Karl Island, a very ma.ssive and coarsely
crystalline porphyritic diorite, is associated with the ordinary grayish
granititegneiss. This rock is of a dark-green colour when fresh, but
near the surface is decomposed for a depth of nearly two inches, the
decomposed layer being much lighter in colour. Large phenocrysts of
deep-green hornblende, some of which are an inch or more across and
most of which possess tolerably well defined crystalline outlines, are
developed in a coarse-grained groundmass composed almost wholly of
allotriomorphic individuals of dark-green trichroic hornblende, the
small and irregular interspaces being filled with felspar and quartz.
Much of the hornblende includes dark schillerization products. The
decomposed layer near the surface shows the somewhat abundant
development of epidote at the expense of the hornblende, giving the
prevailing yellowish-green colour to this portion of the rock. The

MATTAWA RIVER.

213 I

whole exposure measures about fifteen yards long by twenty-five yards
wide and is surrounded by tlie grayisli granitite-gneiss, wliile several
dyk^'s of pegmatite varying from a (juarter of an inch to six inches in
width cut the diorite.

In the northern portions of Hay Baj', the prevailing rock in the Hay Bay.
oidinary granitite-gneiss, the strike of whicli varies from N. GO E. to
N. 70- E.

Rocks on
Sandy Port-
age Bay.

The rock exposed on tlie shores and islands of the bay running
towards the outlet, the north-western portion of which is generally
known as Sandy Portage Bay, is the usual reddish and grayish biotite-
granite-gneiss or granitite-gneiss. The strike varies in general from
N. 50' E. to N. 60° E., while the dip is to the north-west at high
angles, generally varying from G5° to 85°. Near the outlet, the
strike turns more to the north, the foliation in this vicinity running
about N. 40' E., while the bands are nearly if not quite vertical. At
one or two points extremely basic portions of the gneiss were seen to
be highly hornbleiidic, thus passing into quartz-mica-diorite.

Mattawa River.

The term I^Iattawa was first applied to the confluence of this Q|,j^rjjgtpf qJ

river witli the Ottawa. The river has also been known as the Petite Mattawa

Kiver.
or Little l^iver, wliile to the Indians it was formerly known as the

Tessouacsipi. It is really a succession of large deep lakes united by

comparatively narrow and shallow rocky stretches. The total distance

from the Ottawa to the western end of Trout Lake, in a straight line,

is about thirty-six miles, but following the river this is increased to

forty miles. The direction is in general nearly east-and-west, following a

continuation of the main valley occupied by the Ottawa below the con-

tluence of the two streams. In ascending the jNIattawa, rapid water is

encountered almost at once, the stream ilowing over a shallow bouldery

bed. This, together with a small rapid, a little over a mile above at

the outlet of Boom Lake, gives a fall in the river of about two feet.

Boom Lake, the first expansion reached, is only about a mile and a pyoin and

Plein
lakes.

quarter long, and not over a quarter of a mile at its greatest width. I'lein Chant

At the upper end of this lake, the river is contracted in two places to
a width of less than a hundred feet and a fall of nearly twenty feet is
occasioned by the Plein Chant Rapids. Plein Chant Lc*ke at the head
of these rapids, is five and a half miles in length. The widest portion
is near the eastern end, where it is about thirty chains, but this
gradually diminishes westward, till, near the upper end it is not more

Ranidx
aiMi Liic (U's
Aiguillt'M.

Series i)f
raiiids tn
Fimisi Lake.

Talon Chflte.

214 I

NIPI8SIN0 AND TEMISCAMIVO REOIOX.

than three or four chain.s wide. In the widest portion a depth of over
two hundred and eighty feet was found.

Between this lake and Lac des Aiguilles, the next expansion,
the distance is a little over two miles, and four rapids intervene,
with alternuting stretches of still watiw' ; the combined fall is eighteen
feet. Tlie three largest rapids ate known in ascending orilei' as Les
Epine.s, La Rose and Des Roches or Des Aiguilles. The Amable du
Fond Jiiver, the largest tributary of the ^fattawa, enters from the
south side a short distance above the second rapid. Lac des Aiguilles,
which is a little over a mile long and a (juarter of a mile wide,
is separated from the next succeeding stretch of river, lying parallel
to it on the north side, by a rocky bar known as Ties Aiguilles
Islands. The three narrow rocky ciiannels formed by these two
islands, even at high water, barely afford a passage to loaded canoes.
The eastern one constitutes the main route, and a small rapid
at this point shows a descent of a few inches. Above tliis is a
long stretch of deep water that gradually diminishes in width. The
river throughout this distance of two and a half miles is flanked on
either side b}- almost perpendicular walls of gneissic granite.

At the end of this stretch, the upward course of the river changes
sharply to a southerly direction for about two miles, and presents a
.series of rapids with intervals of deep water, the total fall being fifty-
five feet. The Chute des Paresseux, where the water falls thirty-four
feet, is the first and largest of this series. Pimisi or Eel Lake (some-
times also called Penice Bay and Moon Lake) above these rapids,
marks another change in the course of the stream, which from this
place to the head of Talon Lake trends north-westerly. Between
Pimisi Lake and Talon Chute, the river flows for three-tjuarters of a
mile through a narrow rocky caiion inclosed between perpendicular walls
of granite. Talon Chute is the greatest single fall on the 'VNole river,
the water descending forty-three feet over a rocky ledge oouipused of
massive Hesh-red gneissoid granite. The main channel is r a the north
side, but in addition, there is another though much smaller parallel pass-
age. The downward extension of this passage is continued in a deep
gorge which connects with the main channel a short distance lielow the
falls, tlie whole apparently representing the erosion of a band of crystal-
line limestone that here occurs. About half a mile below Talon Chute,
a small rapid occurs with a descent of less than a foot, and a short dis-
tance above it is Talon Lake. To the left, on entering the lake, a
large bay runs westward for about three miles, Kabiskaw Bay at the
western extremity of which an important tributary (Kabiskaw Creek)

BARLOW

]

MATTAWA IMVEU.

!15 I

onters, foriniHg the outlet of Nasbonsing Luke, a large ami irregular
sheet of water situated in the southern part of the township of Ferris.

Talon Lake lies north-west and south-east, ia about seven miles long TiUoii Luko.
and has in general a breath of almost three(|" irters of a mile. The
sliores are generally bold ami rocky, although occasional small sandy
llats occur. The general depth may be said to vary from fifty to one
hundred feet, but in occasional spots a depth of two hundred feet and
over was met with.

The connecting stream between Talon and Turtle or Lower Trout 'Pal"ii to T\ir-
Liike, the next expansion in the river, is about four miles. The stream
leaves Turtle Lake about a mile fron: the eastern extremity. It is
shallow, rocky and rapid with some small intervening ponds of deeper
water. Turtle Lake lies nearly east-and-west and is about four and a
half miles in length and not more than half a mile in width. Thence
iui ascent of barely a foot occui's, in a short channel, l^ Trout Lake, at Trout Lake,
the summit. This is eight and a half miles in length with a greatest
breadth, near the upper end, of about two nules. It is often over 200 feet
deep, and the shores are rough and rocky. To the north of the lake,
a range of hills from three to four luindrod feet high extends with
almost unbroken continuity to the mouth of the Mattawa River and
tlu'i.ce northward and north-westward up the valley of the ()ttawa.

Tiie extreme west end of Trout Lake is only about three miles distant Route thence
from Lake Nipissing, and the neck of land separating the two lakes is j,';',,^,'^ " ^ '''
in general very level. The canoe-route usually followed to Lake
Nipissing, leaves Trout Lake in a bay running to the south near its
western end. The first portage runs over a ridge of sand. The Riviere
do la Vase is then utilized all the way to Lake Nipissing, a distance of
a little over six and a lialf miles. This small stream runs through low
and often marshy ground most of the way, entering Lake Nipissing
about six miles south-east of North Bay.

The land in the immediate neighbourhood of the ]\Lattawa River ciiiinicter
is generally rocky, barren and unfit for agriculture. A short distance "f ''^"*''
from this river, however, in the townships of Papineau, Calvin, Banfield
and Ferris, considerable areas have been cleared, and good progress has
already been made in the settlement of these townships.

The rocks exposed along the Mattawa are for the most part massive Kocks seen

reddish granitite-gneisses, the strike of the folation running in a series "'""I? the Mat-

. . ... tawa.

of widely undulating curves in a general east-andwest direction with

a prevailing southerly dip < 35° to 65^. Crystalline limestone is Liinestones.

very sparingly present in association with these gneissic rocks, and

''^il

216 I

NIPISSING AND TEMISCAMIXf REGION.

' '■:?

Gneiss of
Trout Lake.

Size and fdi'ii,
of LakeNii)is
sing.

Elevation.

Coasts and
islands.

wherever noticed the evidence seemed to show that it has been caught
up in the gneiss during the irruption of the latter. On the .south shore
of Talon Lake, as well as in tlie southern channel at the fa,ll.s, at the
outlet of t( s lake, the crystalline limestone was found in association
with a very massive indistinctly foliated granitite-gneiss, the intrusion
and later age of the latter being apparently clear. Near the western
end of Nasbonsing Lake, the rock is a light-reddish granitite-gneiss com-
posed chiefly of felspar, with a small proportion of giayish quartz and
a little black mica occurring in isolated areas of aggregated scale.s,
together with numerous small garnets. The striks is to the north-west
with a dip to the south-west, generally at a high angle. Near the
eastern end of the lake, the gneissic rocks present are more highly dif-
ferentiated and occur in irregular curving bands which have a general
strike curving gradually around from east to north-east.

On Trout Lake, the granitite-gneiss occurs in reddish and dark-
coloured bands which have a prevailing direction of nearly east and-
west, gradually bending round to the north-west in the western part of
the lake, while the dip is to the south < 45° to o5'.

Lake Nipissing.

1 This important lake has an ai-ea of 345 square miles, and is wholly
surrounded by Laurentian rocks. Its main length is east-and-west,
and its greatest length, from the shore at East Bay, near Callendar
station to the western end of Bear Bay (west arm), is sixty miles ;
while the greatest width, from Beaucage Bay on the north to the
moutli of the South River, is sixteen miles. The elevation above sea
level, at different seasons, varies from 642-2 to 649 '5 feet. The
northern and eastern shores are in general low and for the most part
present sweeping beaches of sand, separated by rounded points of rock.
The water, for a considerable distance from the shore, is shallow. The
west end of the lake has an irregular coast line with long arms and
bays extending and rocky islands. A great number of these
islands strew the more open water outside, running in long lines,
more or less parallel in direction with the peninsulas or points
which divide the bays from one another. The islands, generally
small, are sometimes several miles in extent. The southern shores arc
bold and rocky and the water is deep even in their immediate vicinity.
The whole of the eastern end of the lake is wide and exposed, con-
taining only two small groups of islands known as the Manitou and
Goose Islands.

•J

LAKE NIPISSING.

217 I

The weatern end of the lake consists of four principal bays or Bays at wost-
arms, separated from one another by rocky promontories, their con- j.^j^^,
tinuation towards the deeper water in the central portion of the lake
being marked by the occurrence of long lines of islands and reefs.
The most northerly inlet, McLeod or Goulais Bay, has an almost
direct north-and-south trend. It is about four miles in length by
neaily two in breadth and lies immediately west of the marshy delta
of Sturgeon River. The water in this bay is very shallow. A
rather narrow and crooked channel, however, exists near the eastern
shore, but is navigable only for very small steamers or tugs. Immedi-
ately south-west of this bay and separated from it by the rocky
peninsula ending in Goulais Point, is another arm of the lake, divided
to the west into two subsidiary bays, known as the North-West Bay
and Middle West Bay respectively. North-West Bay is over four miles
in length, with a width rarely exceeding a quarter of a mile, and
having the general direction indicated by its name. Gradually taper-
ing westwards, it receives a small stream that drains some marshy
lakes situated in the north-western part of the township of Macpheraon.
Middle West Bay is much less important, being only about two miles
in length, and at the west end receives a small tributary known as
West River, that drains the southern part of the township of Mac-
jiberson.

Of the indentation extending to the west, however, the largest is West arm or
known as the West Arm or Bear Bay. The general trend of this
extension is nearly east-and-west. An inspection of the accompany-
ing map will convey a good idea of the close depcmdence of topo-
graphical outline on the strike of the foliation of the inclosing
gneissic rocks. In many instances abrupt changes in direction are irrep ilar
encountered, but these follow correspondingly sharp curves in the f'"'"'
lines of foliation and cleavage. The width ot (he bay i ■ very variable,
alternately contracting into narrow straits only a few chains in width
and opening again into wide expanses generally crowded with islands.
T.n the eastern portion for a distance of nearly eight miles, the
average width is nearly two miles. The bay gradually nairows
towards the west end where it receives the waterc of a small stream,
draining several important expansions to the west.

Several important streams enter Lake Nipissing. The largest is Streams enter-
the Sturgeon River, draining about 3000 stjuare miles of country to '"*'' ''^'^ '*'^'''
the north and west, and joining the lake in the midst of a large marsh
on the north side. This low tract of land, forming a delta, has be< n
produced by the gradual accumulation of detritus brought down 'y
the stream.

<■*■-

'!'

(

;'i

'ill;

.1: V

218 I

NIPISSING AND TEMISCAMINO REGION.

; I

■: ) ■

Little Star- The Little Sturgeon or Silver River, enters the Great North Bay

*^^°"' with a swift and deep current, being navigable for canoes, without

interruption, for a distance of a little over two miles from the lake,
where the stream becomes very small and rapids occur. The general
course is at first nearly north, and the upper course i.s nearly north-
east, to its sources in the southern part of the township of Blyth.
Duchesney and Ohippawa creeks enter the lake in the vicinity of
North Bay. The Riviere de la Vase or Little jNIattawa, flows into the
lake about five miles south-east of North Bay. Other important
tributaries enter the lake from tLa south, but these are beyond the
V.'uve River, boundaries of the present map. The Veuve River is an important
stream which enters the west side of McLeod Bay, draining a large
tract of land, the .sources extending westward almost to the Wahna-
pitae River.

Several important islands and groups of islands occur, lying out
towards the middle of the wide eastern portion of the lake. The
most important of these is the group named the Manitou Islands.
These are five in number, situated five miles south-west of North
Bay. The largest is known as the Great Manitou or Newman
Island. It is an irregular triangle in form and about a mile across.
McDonald Island, the ne.xt in size, is about half a mile in length
from north to south but only a few chains in width. The other three
islands are much smaller.

Goose Islands. The Goose Islands lie toward the centre of the open part of the
lake, about six miles west of the ^lanitou Islands, and about twelve
miles west-south-west of North Bay. The largest island is known as
the Great Goose, and is nearly a mile long with a trend of east-
and-west. To tlio west and north-west of these there are aVjouc a
dozen smaller ones, some of which are merely rounded hummocks of
rock.

Manitou
Islands.

Country and
rocks of west
end (if lake.

The general aspect of the western end of Lake Nipissing is rocky
and desolate. In many cases the sparse soil overlying the rarely
concealed hummocks of rocks, atlbrd substance to a rather thin and
scrubby growth of red pine, while the level spots are for the rao.st
part occupied by vast marshes, but some snniU tracts of level land
occur along the banks of some of the tributaries, notably the one
situated on the south side of Bear Bay near its entrance. The
northern shores of the lake, however, border large areas of cultivable
land. The rocks are generally well exposed, especially in the western
and southern portions of the lake. They include the prevailing
varieties of granititegneiss and hornblende-granitite-gneiss, the former

ii|>^

•]

LAKE NIPISSING.

219 I

being the prevailing type. These are cut by dykes and masses of peg-
matite presenting the usual characteristics.

The Manitou Islands are composed of a rock which is remarkably Kocks of the
uniform in composition and appearance, being a medium-textured jsjands?
reddish gneiss, that has evidently been subjected to intense
dynamic action. It has a rather indistinct blotchey appearance,
due to irregular bands of chloritic and epidotic material running
through it, resulting from the alteration of the bisilicates. The micro-
scope shows that the rock has everywhere been greatly granulated.
Its chief constituents are quartz, orthoclose, plagioclase, hornblende
and biotite, with epidote, chlorite, calcite, sericite, iron ore and
apatite. It is thus a hornblende-gninitite-gneiss which has suffered
great alteration, the felspar being turbid and full of inclusions of
sericite, calcite, etc., resulting from its decomposition. Numerous
irregular patches of calcite are scattered through the section. Both
felspar am^ c^uartz extinguish very unevenly. Hornblende is the^most
aba/i'! lilt iorri)magnesian mineral present, but it has suffered such
extreme alteration to chlorite and epidote as to mask its true char-
acters. Biotite, largely altered to chlorite, occurs intergrown with
the hornblende. The section is traversed by numerous cracks tilled in
with secondary quartz, epidote, iron oxides, etc.

On several of the islands, this rock, which has evidently resulted Crystalline
from the crushing of a hornlilentle-granite, contains large patches of ''•"'^'^'^o"^*
pinkish crystalline limestone ; the latter, however, doubtless represents
portions of the clastic Grenville series. The gneissic rocks are inter-
sected by dark-greenish dykes of basic material previously described
in that portion (■* the report treatin^^jf post-archiean eruptives. On
several islands ujuil onMiers of the iiirds Eye and lilack lliver
formations are exj.:.,'sei!, as elsewlnu'e noted.

liock cxposi'V- .liT abundant on the Goose Islands, showing a Hocks of
medium-grained red .granitic gneiss. The foliation is determined by """"" '''*"'*'
the parallel arrai geuient :.i the little bands of biotite. The principal
constituents are (iiartz, orthoclase, plagioclase, microcline and biotite,
with small quanMties of apatite, zircon, chlorite, epidote, sphene,
calcite and secondary iron ore. It is one of the typical biotite- Constituents
gneisses or granitite-gneisses of the region, evidently resulting from "f *'"^ k"i''»*'-
crushing and ilifferentiation of a granitite. The felspars are exceed-
ingly turl)id, 5<f.iiig filled with dust-like particles and contrasting
sharply with lo- clear quartz grains. Orthoclase predominates, but
plagioclase (alul • • '^ very abundant. Most of the micro^'ine grains
observed exhib'l. . moire-structure rather than the typical rectangular

Mil

1. ,

'! -

i
i

i 1

220 I

NIPISSIXG AND TRMISCAMING REGION.

i I

The Sturgeon
River.

Its I

Mouth of the
river.

lattice structure. The biotite shows alteration to chlorite with de-
velopment of secondary magnetite along the cleavage-planes. Apatite
and zircon are both abundant in large well-formed crystals, as well as
irregular grains. Numerous skeleton forms are scattered through the
section, filled with calcite and a substance resembling loucoxene.
Their outlines, sometimes rudely wedge-shaped, are defined by minute
granules of a secondary iron ore, which also run along what were
originallj' cleavage cracks. These in all probability represent titanite
originally present in the rock which has undergone almost complete
alteration with formation of calcite and ilmenite. Minute granules of
epidote are present as the result of the alteration of the felspars. The
rock does not present evidence of having been subjected to an intense
degree of pressure, for although both quartz and felspar have wavy
extinction, the quartz grains are onl i s.'ightl^i cracked and not granu-
lated to anv e.xtent.

Stukgeon River.

The Sturgeon River,* one of the largest in the country to the north-
east of Lake Huron, possessing a drainage area of about three thou-
sand square miles, takes its rise bej'ond the region covered by the
accompanying map-sheets, and close to the sources of the most easterly
branch of the Montreal River. From the source to its mouth on Lake
Nipissing, the river measures about one hundred and forty n^.iles in
length, the general course being to the south-east. At a distance of a
hundred and twenty-five miles from the mouth, the stream is divided
into two branches inconsiderable in size. The more westerly of these
has n(?ver been explored, but the branch which comes from the north-
east drains an important chain of lakes forming the well-known canoe-
route to Shusawagamingt (Smoothwater) Lake at the head of the
eastern branch of the Montreal River. Three miles below the forks,
the river expands to a quarter of a mile in width for a mile and
a quarter, forming Paul Lake,:]: which is frequently though incorrectly
described as the source of the Sturgeon. This lake is about 1258 feet
above the sea. The Sturgeon debouches in an extensive marsh by two
channels. The most direct or westerly one is almost completely filled
with detritus, while the eastern branch is comparatively deep and
navigable even for steamers. Once across the bars, the river ofTers

* This river is clled "Cluiniiihiin's River " on Delisle'.s map of New France, 1703.

t Simiftinies also called "Wliite IJeaver Lake" from a mountain of that name
which rises immediately to the west of the lake.

t The name is given in honour of " Big Paul," a sub-chief of the Temagami liand of
Chipiiewa Indians, who has m.ade this lake his headquarters for many succeeding win-
ter iiuuta.

■Jt.\

STURGEON RIVER.

221

uninterrupted navigation as far as the village of Sturgeon Falls, over
four miles from the lake.

In ascending the stream the general direction is N. 35° E. for eleven
miles in a straight line. This is to the mouth of a tributary coming
from the east, known as Smoke River, that drains the southern portion
of the townships of Grant and Charlton. In this distance navigation
is interrupted by two falls and two rapids. The tirst of these, Sturgeon Sttirjfeon
Falls, is opposite the village of the same name, at the intersection
with the main line of the Canadian Pacific Railway. Sandy Falls is
the name of the next, nearly six miles above the village, while the
rapids, which occur a couple of miles beyond, generally require to be
portaged in the ascent, although they can be run in descending. The
portage to avoid this half-mile of broken water is on the west side of
the stream.

Near the mouth of the Smoke River, the Sturgeon takes a sudden Cmirse of the
bend, and has an upward direction in a straight line of N. 61° E. for above^Sinoke
28 miles, as far as the " Elbow," in the township of Janes. Fol'oN^ing Kiver.
all the sinuosities of the stream, however, this distance is increased to
a little over thirty-six miles. The main tributaries in this interval are
from the north, draining large lakes in this direction. The Temaganii, Temagami
which is a very turbulent and rapid stream, is the largest feeder of the ^'^•^'''•
Stu -geon, and is the principal outlet of the large lake of the same
name. It enters the Sturgeon a little over twenty-three miles above
the mouth of the Smoke River. The Tomiko (contraction for Otanacora- TomikoRiver.
agosi or Canoe-making) River enters a little over five miles above Smoky
Falls, deriving most of its water from several large lakes situated in
the townships of Gladman and Hammell. The lower portion of the
stream, from Tomiko Lake to the Sturgeon, is rarely if ever used for
the purposes of canoeing. A long portage to avoid this rough stretch
of river, runs northward from the Sturgeon, starting from a point nearly
two miles above Smoky Falls. Tt affords an entrance to Cameron Lake
and thence through Chebogomog Lake into Tomiko Lake. The upper
portion of the river, however, is travelled to reach the numerous lakes
situated near the head-waters of the sevei-al branches of the stream and
thence to the region beyond. Pike River is another feeder, coming
from a lake of the same name, situated near the centre of the town-
ship of Bastedo.

Between the mouth of the Smoke River and the " Elbow ", the Stur- Smoke
geon is broken by one fall and five rapids, the latter all situated above kHjow.
the mouth of the Temagami River. The most important of these
obstructions is the Smoky Falls, where the river descends over a solid

i '■ :■■:'!

;;||

Ur ml

jf M

'4 U

'is 131

1 -r

T'!l

il I

1^ i

'k ■

^^rr

222 1

NIPISSING AND TEMISCAMING REGION.

ill- !

Sturgfon
River aliove
the Elbow.

Navigability
of the river.

Cultivablt
land.

Rocks.

barrier of gneiss for more than twenty feet. The portage runs over a
small rocky island of gneiss which here divides the river into two
channels.

At the " Elbow," the trend of t'.d river again changes abruptly to a
direction of N. 14° W., which course is maintained as far the mouth of
♦^he Obabica River, a distance of twenty-two miles increased to thirty-
four miles by the bends of the stream. Only a little over a third of
this distance is included on the accompanying maps, as far as the mouth
of the outlet from Wawiash-Kashing and Manito-Peepagee lakes. The
largest tributary in this distance is the Maskinonge River, that reaches
the main stream from the west about two and a half miles above the
" Elbow " and drains a number of large lakes, shown on the Sudbury
map sheet (No. 130.)

The Sturgeon River is in general readily navigable for canoes
througnout the whole distance embraced in the present map-sheets,
although the current is strong neaii y the whole way. Between Smoky
Falls and a point about three miles above the mouth of the Temagami
branch (a distance of about twfii ':y-f3ve miles) there is no greater
impediment to canoe navigation thau the 'Strength of the current. The
river, except where contracted at the rapids and falls, varies in width
from a little over two hundred and fifty feet near the mouth to about
a hundred feet in the township of McNish near the north-west corner of
the Lake Nipissing sheet. The depth varies from three to twenty feet,
with an average of perhaps ten or twelve feet.

The flats along the river are liable to inundation during the high
spring freshets and the actual rise in the water at the several points
iiong the coarse of the stream, may be readily ascertained by a reference
CO the appended list of elevations.

The river for the most part pursues a somewhat tortuous course
through a tolerably level flat of considerable extent, exhibiting numerous
sections of a stiff grayish clay overlain by coarse yellowish sand, in the
immediate valley of the Sturgeon. Below the Temagami River there
are many areas of considerable extent which have been utilzed for settle-
ment and the soil has in general proved productive. Between the
mouths of the Tamagami and Maskinongt' rivei's, these flats are fewer
and less extensive while the county immediately adjoining becomes for
the greater part poor and rocky. Above the Maskinonge, very little
land is available for farming, the country assuming a broken and
mountainous character.

The rocks throughout this distance present the usual characteristics
of the reddish and dark -grayish gneisses. The dip is towards the south

THE MONTREAL HIVER.

223 I

or south-east at an angle of often considerably less than 45\ The
exposures in the immediate vicinity are very few, and except in the
neighbourhood of falls and rapids are small, consisting chiefly of rounded
hummocks protruding from the overlying drift material.

The contact between these rocks and those of the Huronian, occur- Junction of
ring to the north-east, crosses the Sturgeon River a short distance above jmd Hmon'ian.
the " Elbow". The actual junction is not visiblfi, but exposures of the
Hesh-red granite-gneiss of the Laurentian and the light greenish com-
pact quartzite of the Huronian occur within a short distance of one
another.

The Montreal River.

The Montreal River is, next to the Ottawa and Sturgeon rivers, the
largest stream included within the area covered by the present Report,
draining an area of about 2500 square miles.

The general course of the river, so far as it is included in the Lake (Jeneial
Temiscaraing sheet, is south-east, and the length almost forty-seven treal Rher
miles in a straight line. This may be divided into three parts, the
first and third of which are approximately parallel in direction, w. 'le
the second, or short intervening stretch lies almost at right angles.

Ihe lower portion of the river, from Lake Temiscaming to Mud Lake Lower part of
portage, is now superceded as a canoeroute by the shorter and easier
passage by way of Haileybury, Mud and Sharp lakes. There are
numerous rapids, and the river, throughout this distance, flows in a
narrow valley, generally from 400 to 450 feet deep. Only a few small
streams enter this portion of the river, as the highest land occurs in
close proximity to the banks on either side. The lowest three miles
of the river, before it reaches Lake Temiscaming, is a series of rapids
with a fall of 160 feet. At the "Notch," near the mouth, the river The Notch,
tlows through an extremely narrow channel, with rocky perpendicular
walls, composed of dark-greenish greywacke slate, much jointed and
broken. This gorge has a breadth varying from sixteen to thirty-three
feet and is a little more than a hundred yards long, with perpendicular
walls about forty feet high. The rapids above referred to are overcome
by a portage about three miles long.

For about six miles above this portage the river is crooked, Rocks seen.
with a fairly gentle and uniform current, its channel being cut through
a narrow plain of stratified drift material. There are only occasional
outcrops of rock, and these show a comparatively fine-grained arkose,

Htc Plate IV.

i 1 '!}

j t

i-i

|1 'L

I'r

't '

;i I'

\ ,

tmi

: \

224 I

NIPI8SINO AND TEMlSCAMINfJ REGION.

Fountain Fall
and Kagg"(l
Clmte.

Hound Chute
to Mud L;kko
portage.

Rocks near
Mud Lake
portage.

20'. Two more rapids of considerable dimensions
3tween Kaj^ged and Hound chutes, having a

forming the transitional beds upward from the greywacko and slate to
the (juartzite grit that characterizes the summits of the hills extending
westward to Bear Lake.

Three rapids occur in the next stretch, before Fountain Fall is
reached, the total fall in this part of the river being over thirty feet.
The rock, wherever exposed, is a dark-green somewhat coarse diabase
or gabbro, the felspar, especially in the coarse phase, being frequently
of a reddish colour. Fountain Fall has a sheer descent of twenty feet
over an outcrop of breccia-conglomerate. Ragged Chute is situated
a short distance above, and has a fall of about thirty feet. The
hills on either side of this wild rapid rise precipitously from the river,
and the portage, which is situated on the north-east bank, runs over a
very high and steep hill, The rock exposed is the usual breccia-con-
glomerate, showing a dark-green chloritic matrix which is often pres-
ent in comparatively small proportion, in which is embedded an abund-
ance of fragments of felspar, granite and diabase. About a mile above
Ragged Chute, the slate is superimposed upon the conglomerate,
dipping H. 70' N. <
occur in the spaces ^v.^.-..^ ^".5,5
combined fall of thirteen feet. At the latter place, the waters of the
river make a clear leap of twenty-five feet, over an outcropping ledge of
diabase. From the head of Hound Chute to Mud Lake portage, the
banks on either side of the stream, and especially that on the north-
eastern side, exhibit perpendicular cliffs composed of diabase, greatly
resembling and co-extensive with a large mass which reaches the west
side of Lake Temiscaming, there forming the cliffs known as the Mani-
tou and Devils Rock. The current in this interval of nearly five miles
is very swift, showing a total fall of about eight feet, but with no dis-
tinct rapids.

Immediately below Mud Lake portage is a high hill of diabase that
rises precipitously from the water on the north-east side, while a short
distance above, on the opposite side, smaller elevations composed of
similar rock were noticed in close proximity to the stream. In the
vicinity ot the first rapid above Mud Lake portage, the banks are again
high and rocky, composed oi the coarse diabase or gabbro with much
fresh-red felspar, giving it f-omewhat the appearance of a basic granite.
A small rocky island about twelve chains below the rapid, shows this
diabase to possess a very perfect series of jointing planes with a direction
of N. 50° E. and dipping S.E. <70°. The strike of these planes
corresponds closely with the trend of the stream at this point and may
have been the cause of its direction. The rapids, which are very strong,

BARLOW.

•]

THE MONTREAL RIVKH.

) I

liave a f.iU of seven feet, and are caused by a barrier composed of out-
cropping ledges of the diabase aided by an accumulation of loose
lioulder material. There are no exposures of rock Ijetsveon the head of
these rapids and Bay Lake, while the river, between the two other inter-
vening rapids, is marked by the occurrence of comparatively wide lake-
like expansions, which in places show a considerable current.

Bay Lake, known to the Indians as Pakeegama or Mattagamashing, r.ny ],uk.
occupies a rather deep depression in the rocky plateau, being bounded,
especially on the south-west side, by high rounded hills of slate and
quartzite. It runs in a north-west and south-e.ist direction, with a
length of seven miles and an average breath of a little over a quarter
of a mile. A largo bay near the north-western extremity runs in an
easterly direction for about two miles and a half. The portage froin
Loon Lake, on the road to Temiscaming, reaches the north-east corner
of this bay, while the Hudson's Bay Company's post is situated on the
point on the north-west shore of the lake near the entrance to Portage
i;ay.

The south-western shore, near the south-western end oT Bay Lake, itnck

.Xdt

shows excellent exposures of well banded and evenly jointed greenish- "',',','i'^i'f^y>.iJ^"*
grey slates, while the north-eastern shore in tliis dircctitjn is low and l-akc
covered with thick green bush. About a iin'le and a quarter north of the
outlet, the slates are overlain in conformable sequence by the yellowish-
green quart zite-grit, the whole having a north-westerly dip < 5° to 12\
The slate as usual shows a gradual transition througli a more massive
slate into a grcywacke or felspatliic sandstone, which merges upward
into the comparatively coarse-grained arkose sandstone or quartzite-
grit that rises into hills varying from 250 to 300 feet above the lake,
in places forming precipitous cliffs of considerable height.

A specimen of this rock was examined by the late Prof. G. H. Williams LitlioUwical

and was taken to represent the transitional portion near the immediate fjiaract^ r uf

^ ' the sliitr.

junction between the coarse greywacke and the quartzite or arkose.

The small hand specimens showed a banded coarse and fine conglomer-
atic sandstone or greywacke. The coarser portion of the specimen
presents the ordinary characters of the prevailing quartzite-grit,
liolding good sized fragments of (juartz both angular and rounded in
outline, embedded in a moderately abundant sericitic matrix. The
finer-grained portion, which has a somewhat darker hue, is a rather
typical greywacke, showing " an aggregate of angular and sub-angular
quartz grains with some felspar. Betsveen these grains much chloride
has been developed, which, together with the magnetite present, gives
the dark colour to this layer."
15

!:i

1 i l:

;ll

226 I

NIPISniXG AN'D TEMISCAMING HEfJION.

Quartzito and
eke.

Dialmso of
Fort ago Bay.

Bay Lake to

Mountain

Lake.

This quartzitp, as usual, occurs in very tliick find massive beds and
the dip cannot be nia'Io out with any certainty e.xtept in a few places.
It is exposed all along the suuth-west shore of the lake as far as the
inlet and forms the south-western portion of the puint that separates
Portage Bay from the main body of the lake. Fuither up the river
this rock is underlain, first, by a massive brownisli greywacke orslatf,
exposed a short distance below Pork Rapid, and next, in descen'ling
order, by the well banded greenish slate.s, dipping 8. 55° E. < 10' to
15°, which continue as far as and a little beyond the inlet from Laily
Evelyn Lake. Tlie .structure is therefore tiiat of a somewhat shallow
syncline, the basal bed being represented both by ihe banded slates
exposed in the south-eastern part of Uay Lake and thosci occurring in
the vicinity' of the outlet from Lady Evelyn Lake, the overlying
quartzites resting in the trough thus formed.

The point on which Bay Lake post is situated, is composed of
coarsely crystalline diabase or gabbro, the felsj)ar frequently possessing
a distinct flesh-red colour. The massive and rounded exposures of this
rock are cut by irregular ramifying dykes, composed of a fine-grained
pale-grayish or pinkish aplite. This basic irruptive forms the shores of
Portage Bay, as well as the north-eastern part of the point separating
this bay from the main body of the lake. To the northwest of
the lake, it continues for a considerable distance inland, forming a
series of high, though i-ounded hills in this district, while to the east,
as far as can be learned from the occasional outcrops, it is continuous
with the mass which forms the southern part of Sharp Lake extending
as far as the western shore of Lake Temiscaming.

Between the head of Bay Lake and the head of Lady Evelyn Lake
(Mattawapika), the river is in general a line, wide stream, with occa-
sional short stretches of swift current. Pork Rapid (Kokooshbuwatik),
has a total fall of nearly seven feet, the portage being on the south-
west bank. The north-eastern banks of the river are low, and the
country for many miles is flat and swampy. On the south-east side
in that direction there are only occasional low rounded exposures of the
greywacke and slate, and these are situated some distance away
from the stream, forming a series of rounded hills. Between the
Mattawapika and Rounder Mountain Lake the river is, as a rule,
wide and navigable, with only two interruptions by rapids One of
these is a little over a mile and the other about four miles below
Round Lake, the portage in both cases being on the northern or north-
eastern bank of the river. The combined fall of these two rapids is
about eight feet, the upper one being the larger with a descent of five
feet.

lARLOW. J

THE MONTREAL UIVEK.

227 I

The shores in the vicinity of the Mattawapika, show exposures of
a well banded slate which dips S. 55" E. < 10' to 15", and
Cdntinueb for ahout a mile above this f)oint, where it is interrupted by
a mass of diabase or gabbro, which, on the south-east side, rises into a
series of precipitous hills. This rock may extend across the stream to
the northward, but any hills on this side are much lower and less pro-
nounced, and are therefore more likely to be underlain by the gray-
wacke slate. This mass of diabase extends to within a ([uarter of a
mile of the outlet from Mocassin Lake, and is an extension northward
of the mass of similar rock which forms the western shore of the
last stretch of Lady Evelyn Lake. To the north-west, this diabase is
replaced by the (juartzite grit or ai-kose which forms smaller and less
conspicuous eminences extending northward and inland for some miles ;
while to the north-west, the general surface outline would seem to indi-
cate its continuous presence as far as the south-eastern extremity of
Indian Lake, although no exposures could be seen. The rock is the
u><ual greenish or reddish-gray, coarse arkose, so prevalent throughout
this district. A specimen of this rock was examined by the late
Prof. G. H. Williams, who says that " it shows an even-grained
mixture of somewhat rounded quartz grains with an equal amount of
felspar (orthochi&e, microcline and oligoclase). The minerals and their
proportions are those of a granite, and yet the appearance of the
grains and their relations to one another at once disclose the
clastic character of the rock. The felspar, except a few of the largest
grains, is quite changed to kaolin or sericite, although its external
characters are still plainly discernible."

Indian Lake is only an irregular expansion of the river crossing its
downward course at a considerable angle, and discharging from the
south-west side nearly a mile from the foot of the lake. Near Indian
Lake, the banks are somewhat higher and are composed of grayish
stratified clay, which makes a good soil. The shores of Indian Lake
are as a rule low and grassy, presenting no rock exposures, but the
comparatively high hills that border the south-western end of the
lake are probably composed of quartzite-grit. From Indian Lake
to Round or Mountain Lake, the river flows with a very gentle cur-
rent between banks of iiioderate height composed of stratified gray
clay. As the first rapid is approached, these banks are appreciably
higher, but above the second rapid the area on either side of the river
becomes much lower, while the immediate outlet from Round
Lake is flat and swampy. Both of the rapids below Round Lake
are caused by boulder obstruction. The south-western shore of Round
Lake shows high hills composed of the coarse diabase or gabbro, and

Rucks of Laily
Esflvii Lake.

Microscoiiic
cbiiracter of
grcywacke.

Indian Lake.

Indian Lake
to -Mountain
Lake.

ill

Diabase or
gabbro.

1 ■£

228 I

NIPISSINO AND TEMlMCAMINCi HEniON.

exposures of this rock were noticed on the nortli-enstern side nenr the
outlet, Init to tlie nortli-eiistwiird of the lake the whole region seems to
be comparatively level, the soil beinjj a clay loam. The diabase and
gabbro contains much llesh-rtid felspar, greatly resembling in this
respect the coarser portions of the rock exposed at Quinn Point on
T^akci Temiscaming as well as on the north-east shore of Bay Lake.
When subjected to the weather this felspar kaolini/.es, thus producing
a moderately coar.se-gi-ained rock, closely resenddiiig in macroscopic
appearance a Ijasic hornblendic granite.

TiiK Matahitchouan llivEn.

M'ltiiiiit- The -Matabitchouan and Montreal rivers reach Lake Tennscaming

lIuHMll lIlMT. -11.,, 1. , 1 .

almost at tiie same point, but while the general course of the latter is
from the northwest, that of the Matabitchouan is from the south-west.
The proximity of the moutlis of these two streams has, in the past, been
the cause of some little cont'u-;ioii in the names .Mpplied to each. AL'Ua-
bitchouan seems to have been the original Indian name of the Mon-
treal River, while what has of late years been called the Matabitchouan
is known to the fndians as the Wabos-i.e-mata-bisipi (or Habbit-sit-
ting-down iliver. The name.s have, now, however, become fixed as here
(imployed. The Matabitchouan is one of the most important streams
in this district, and for manv years was the onlv ciinoe-route in com-
Us w.'itiishcd im,u uij(> between lakes Temiscaming and Temagami. Its head-waters
lie to the north and west of White-bear Lake. The smallest branch
takes its rise in Caribou Lake, on the main canoe-route, within a
(|uartcr of a mile of the north-east arm of Lake Temagami, and this
small lake sends another and larger stream into Lake Temagami. The
largest or main branch of the river rises in Mountain Lake, to the
south-east of Annima-nipissing and Bay lakes. Two other branches
of some size drain lakes that lies close to the hills bordering the
lower stretch of the Montreal River, debouching in the north-eastern
corner of White-bear Lake within a short distance of one another.

From the mouth on Lake Temiscaming to Mountain Lake, the dist-
ance, in a straight line bearing N.70' W. is nineteen miles, while follow-
ing the general canoe-channel, this distance is inci-easedto tliirty-seven
miles. This whole space is divided into two main directions of How,
forming an angle of 70' with one another, these constituting two sides
of a triangle, while the third has the length and direction already men-
tioned. The tirst of these stretches, which extends from the mouth of
the river to Rabbit Point on Rabbit Lake, has an upward bearing of
S. 44"^ W. for thirteen and a half miles, although the channel usually

iUld iHllllcllf

liDwer i>art
of Matabit-
«houan .

¥'

■]

THE MATAUlTCilOUAN UI\ EH.

229 I

Lnivclled measures about sixteen miles. Tlifl third side of tlie triangle,
wliicli reaches from Ilabhit Point to Mountain Lake, shows a •,'('n('ral
direction of M. 20 W., with a lfn;,'th of nineteen miles, although the
most direct canoe channel measures about twenty-one miles. From
the mouth of the Matabitchouan to the tirst portage, the river has cut
a fairly deep channel throuijh drift material, the bands on either side
l)('i i|)osed of a stratified gray clay. The strength of tiie current

ill I .nterval varies with the height of the water, for during times of
freshet, the water of the lake backs u|), forming a comparatively deep
channel to within a short distance of the tirst portage ; while, during
(iidinary stages, the stream has a swift current almost to the mouth.
The norihern banks are as a rule much lower than those on the south
side of the stream. A short distance south of the river is a high and Hi'iiver
prominent hill, known us the King of the Beavers, also sometimes cal-
led the Montreal Mountain or Beaver Mountain. Acconling to baro-
iiuarical observations, this hill has an elevation of GGO feet above Lake
Ti-miscaming, or 1248 feet al)ovo the sea.

The sunmiit of Beaver Mountain, for 340 feet, is composed of a | ,,,|.^ fmnid

•'reenish-grey medium textured diabase, much sheared anil broken, ''1 1'":'^''.'''
° ^ . . , . Mountain,

the pi "es of shearing being abundantly coated with greenish decom-

posit >roducls. Below this rock is a gi-eenish slate, which marks

the 1 tnd more gradually sloping portion of the mountain. The

strike of the slates curves around, conforming beautifully with the line

of outcrop of the diabase, dipping into or beneath what seems to be

an irruptive mass of lacolitic origin.

The first, or Matabitchouan portage, occurs a little over two miles Matahit-
frum the mouth of the river, where a series of rapids and falls occur ^g|!. '
with a descent of 200 feet. The stream here describes a sharp
bend to the north, while the portage, to overcome these obstruc-
tions cuts, across the bend thus formed, running over a hill, the high-
est point on the trail being 330 feet above the level of the river at the
foot of the portage. The ascent of the portage is steep, passing iirst
over stratified gray clay, and clay and b(julders, but near the summit
it is rocky. This is the breccia-conglomerate, containing pebbles
chietly of a flesh-red granite embedded in a dark-green chloritic matrix.
The west end of the IMatabitchouan portage comes out on the first of
a series of four Bass lakes, i^urabered in ascending order. These are
s'nidl expansions, united by narrow shallow channels, with an appreci-
able current.

The south-east shore of the Second Bass Lake, consists of high per- Soconci B<asn
pendicular cliffs composed of a fine-grained hornblende-granite, evidently '^ ^*''

I: I,,

I 'ill- i

s^t

■: \

* ■

!l J

;i
!

■ ;-*

I ii

■
l"

i^ M

Rocks of
Tliinl Bass
Lake.

vl.

Rocks bet-
ween Third
and Fourth
Bass bke.

230 I

NIPISSINO AND TKMISCAMING RF3I0N.

an extension of the large mass of somewhat similar rocks coloured as
Laurentian further to the south. At the base of the cliff, near the
upper end of the lake, this granite may be seen in contact with the
breccia-conglomei'ate, that constitutes the basal member of theHuronian.
Precisely similar rock forms the eastern shore of the Third Bass Lake,
but is 80 massive that no lines indicating original sedimentation could
be discerned. A thin section of the finer portiv n, or matrix, of this
conglomerate obtained from an exposure immediately below the rapid
that separates this lake from the next succeeding one above, shows
the rock to be a highly felspathic sandstone or grey wacke, consisting of
subangular grains of quartz, orthoclase and plagioclase with a consider-
able amount of a green chloritic decomposition product occurring for the
mcjst part between the quartz and felspar grains and giving the rock
its general greenish tint. A few grains of pyrite ..re also present.
The majority of the grains are composed of felspar, which is a good deal
decomposed, while the quartz shows evidence of having been subjected
to great pressure. On the western shore of the lake, near the upper or
south end, exposures of greenish banded slates may be observed, dippinj."
to the westward at a low angle and overlying the breccia-conglomerate
of the eastern shore. These slates constitute a belt about a quarter of
a mile in width, and to the west merge gradually upward through a
massive and uniformly fine-grrined greywacke into the sea-green sand-
stone or quartzite-grit that foims most of the shores of Trout Lake, ( a
small expanse of water to the north-west of Third and Fourth Bass
Lakes).

A rapid with a conside''able fall intervenes between the two upper
Bass Lakes. Macdonald Creek, an important tributary, enters the
Fourth Bass Lake from tlie south, draining a number of hakes in that
direction. On the west shore of the bay into which this creek empties,
are high rounded exposures of the breccia-conglomerate, while at the
small rapids at the upper or south-west end of the lako are ledges of
the overlying greenish banded slates, striking about north-east and dip-
ping to the north west.

Fourth Bass Above the Fourth Bass Lake a small rapid occurs, and a short

Lake to Kane- (ligtance beyond five rapids follow in quick succession. During
age. times of low water a portage known as the Ivanebeatika (or A)ong-tlie-

rocks) portage, is made on the south side of the river, commencing at
the foot of a small fall and running for a distance of nearly three-
quarters of a mile. Frequently, however, the passage either up or down
is made by keeping close to the stream and utilizing the shorter
trails. The north side of the-river shows precipitous cliffs of greenish

]

THE MATABITCHOUAN KIVER.

231 I

banded slates, which rise abruptly from the water's edge to a height

of over a hundred feet, having at the base a talus of angular blocks.

Only a quarter of a mile separates these from the Devils Rapiil, 'Hvils Ilapid.

where the water pours through a narrow canon of slate, with a

portage on the south side of the stream. The banded slates here

exposed have a strike of N. 20° E., with a dip to the north-west.

A ciuiet strutcli of similar length separates this from the next succeed- ,V'rV'??T*"i

' . o Kabhit Lakci.

ing rapid, at the foot of which the green banded slates strike N. 64°

E. and dip nort' ^rly < 50'. The upper end of this portage shows

exposures of a somewhat coarse gabbro or diabase, a belt of this rock

about three-eighths of a mile wide crossing the river at this point and

interrupting the slates and greywackes. A stretch of three-quarters of

a mile of comparatively deep and navigable water, with swift current

at only one point, occurs in the interval before the foot of the next

portage, which is the last before Rabbit Lake is reached. This portage

which is a little over half a mile in length, passes two rapids and a chute,

the latter exhibiting a very pretty fall of about fifieen feet at the

immediate outlet of the lake. A specimen obtained at the foot of the

portage is a very fine-grained reddish-gray rock, resembling a felsite

macroscopically.

At the outlet, the rock is a fine-grained greenish-gray felsite orfels- Kock-Knear

..,",,,. * -^ . . . , outlet. )f lake,

pathic sandstone very similar to the last in composition with a

strike N. GO' E. and a dip to the north-west < 50°. It is impossible,

however, to bo sure that these plano,s represent original lines of sedi.

mentation, for a little over a mile to the south of Rabbit Chute, on the

west side of Outlet Bay, the greenish banded slates were seen dipping

abo'i', west < 50' and superimposed upon the breccia-conglomerate

which forms the eastern shore of this bay wherever the rock is seen.

The present name. Rabbit Lake, by which this stretch of water at the Rabbit Lake.
head of Rabbit Chute is known, is an abbreviated translation of the
Indiii.i designation Wabos-na-ma-ta-bi (or Rabbit-sitting-down Lake)
because of the occurrence at one of the most prominent points of
a large angular mass of greywacke which has a fancied resemblance to
a rabbit in a sitting posture.

The lake has a general trend of north-east and south-west, and the
distance from Rabbit Chute to the end of South-west Bay is ten miles
in a direct line, although the distance from portage to portage on the
canoe-route is a little over eleven miles. The a^•erage width of the
lake is about three-eighths of a mile, while its total area is
about eight square miles, and its height about 939 feet above sea-
level. The lake has a rather irregular outline, with a number of large

i I'

■ i \\l I

1'.' '

1 ^il

1 (■. k'.

Ill

Outli'ts of
hlkf.

Dialiasc of
Outlet ll.iy.

Micioscoiiii
clnirafUn'.

Contact \s itli
granite.

232 I

MPISSIXG AND TEMISCAMING REC.IOX.

bays, which are, in their turn, cut up into many smaller inlets.
At the southern end of Outlet Bay, one of these indentations stretches
away to the south-east, crossing tiie strike of the I'ocks for a distance
of over two miles. During extreme high-water a small stream Hows
out of the end of this bay into Ross Lake, at the head- waters (if Mac-
donald Creek, which flows into the Alatabitchouaax River at the Fourth
Bass Lake. The b ly running to the north-west forms a portion of the
main route of travel between Terniscaming and Temagami lakes. With
a gradual curve from the north to the north-west it reaches the foot
of the portage to White-bear Lake, about tive miles from Rabbit Point.
The South-west J3ay is really a continuation in this direction of the
main Ijody of the lake.

Near the southern end of Outlet Bay, a mass of greenstone (diabase
and gabbio) crosses South-east Bay, and, running parallel to Outlet
Bay but a short distance inland, this doubtless connects with the belt
of such rocks tliat crosses the ]Matabitchouan at the third rapid below
Rabbit Chute. This band is a little over half a mile in width, and in
the vicinity of C)utlet Bay is followed by the massive breccia-conglom-
erate, which is in turn overlain by the fine-grained brownish, and
greenish-gray slaty rocks with a strike of N. W. and a dip west
< 20 . This dialjase, as it iiiay be named, is by no means homogeneous in
composition, and patches of granitic aspect and composition occur with-
out any sharp line of division, merging by degrees into the more basic
portion of the mass. In places these granitic patches are cut by dykes of
fine-grainetl diabase evidently of somewhat later origin.

To thesouth of this greenstone mass, a belt of the breccia-conglonierate
comes in, but the actual contact is hidden in a low valley at the foot
of a small bay on the south-west shore. On the south-west side of the
bay, the conglomerate band has a width of a quarter of a mile, but on
the noi'th-eastern shore it is somewhat wider. The matrix is a fine-
grained, compact, dark greenish-gray I'ock, breaking with a conchoidal
fracture. Under the microscope it is .seen to consist of a sery fini'-
grained mosaic of quartz and felspar, filled in with minute scales of
chlorite and sericite and granules of epidote. In this are scattered
larger fragments of quartz, orthoclase, phigioclase, luicrocline, horn-
Ijlende, l)iutile (both the latter minerals largely altered to chlorite) and
sphene. In this fine-grained portion are imlieddcd occasional pebbles
and fragments often of considerable size, composed, chiefiy of red and
gray granite. Near the contact with the granite rocks to the south,
the rock is seen to have undergone extensive deformaticm by pressure,
the resulting shearing-planes being abundantly coated with the usual

OvV. I

THE MATABITCIIOUAN RIVER.

133 I

n-iito

the
it on

filU'-

oid.i'i

fin-

•s ot

be red

llOI'U-

aml
luul

)Utll,

irc,
isual

I ■ i
■ »1

greenish products of decomposition. The pebbles themselves, which
are relatively much more abundant, are seen to have been stretched
and rolled out as a result of such extreme dynamic action ; while a very
marked foliation has been developed in the finer-grained portion of the
rock, which is seen to wrap around and conform as closely as possible
to the outline of each individual fragment.

Besides these lengthened pebbles there are granitic inclusions, (iiunitic
running for the most part with the cleavage, but which in most cases "','„^\ynu''r:iU'
present a somewhat more irregular and indistinct outline. These
appear to be of the nature of small apophyses of granite, although
it is exceedingly dithcult to discriminate in every case between
these irruptive dyke-like intrusions and the distinctly rolled fragments
which have been considerably flattened as a result of pressure. The
cleavage or foliation of this conglomerate has a direction varying from
S. 18" W. to S. 21° W., with a prevailing south-easterly dip at a high
angle.

The junction between this rock and the granites and gneisses Junction of
exposed to the south, was seen crossing the lake about three-quarters lnl^mle[J^>a!
of a mile from the foot of S(nith-east Bay. The line of outcrop of the
granitite-gneiss seems to form a considerable angle with the planes of
foliation of the conglomerate, intersecting these in a direction of S. 53"^
W. Further to the south, the granitite-gneiss is considerably mixed
with a much more basic rock, doubtless either a gabbro or a gabbro-
diorito, which, however, appears to have been an integral portion of the
.same magma from which the granitite-gneiss has solidilied. The gneiss
is, as a rule, very granitoid in aspect, sometimes very coarse-grained
and even porphyritic in structure, while in other places not far distant
it is of medium texture and distinctly foliated, this structure being
determined by tlie alternation of reddish and greenish-yellow bands.
The strike of this foliation varies from N. 23' E. to N. 33' E., while stnict>ue of
the dip is to the north-west <45'' to 50°. Under the microscope, a y^'"'"^'*^'''-
precisely similar rock from the South-west Bay is seen to be a granit-
ite-gneiss, composed of orthoclase, plagioclase, quartz, chlorite (derived
from Ijiotite originally present) and epidote, with small quantities of
sphone, apatite, and secondary calcite. The alternation of reddish and
greenish-yellow bands so characteristic of this rock, is due to the par-
allel disposition of certain layers of felspar stained by iron oxide,
with others in which the felspars present have undergone exten-
sive saussuritization : the resulting scales jind granules of sericite and
epidote arranging themselves in a more or less definite position at right
angles to the direction of pressure. This granitite-gneiss, and associated

4 •;

il" ■ )'m. *!, ■lis

iili

234 I

NI PISSING AND TEMISCAMING RBaiON.

Contact of
irruptivo
charactfi' .

Southern
tihore of
Rabbit Lake

granitite, with a much smaller proportion of "greenstone," occupy all
of the southern end of South-east Bay, and is continuous with the
large mass of essentially similar Laurentiau rocks exposed in the region
to the south

The contact between the granitite-gneiss and the slate-con-
glomerate is very evidently of an irruptive character. The slate-
conglomerate is everywhere, near the line of contact, much squeezed,
and is in places penetrated by small dykes of the irruptive rocks ; while
fragments of the former may be seen caught up and embedded in the
gneissic-granite, even at a considerable distance from the line of junc-
tion, on both sides of the bay. Near the line, the matrix of the con-
glomerate is much hardened, as a result of such igneous action, or reu-
dered much more chloritic and epidotic as a result of the preaence and
percolation of heated waters. On the north-east slu^re, near the con-
tact between the two rocks, the foliation of the granitite-gneiss dips to
the nortli-wost < 30', while the conglomerate has an almost if not quite
vertical attitude ; although further to the north it dips to the north-
west < 50".

The southern shore of the main body of Rabbit Lake, is composed of
a very distinctly and evenly bedded slaty greywack^, of gray and
greenish-i'ray colours, the greenish colours being due to the relatively
gre iter abundance of sericite and chlorite. The strike varies from
N. 18° E., on the shore opposite Rabbit Point, to N. 40" E. near the
north-eastern part of the stretch, curving gently with the trend of the
shore. The banks rise rather abruptly fi'om the water's edge, in places
forming low vertical cliff's of slate, especially ne.u- the north-eastern
portion. The effects of glaciation are very marked. The graywacke-
slate rests conformably upon the breccia-conglomerate which forms the
north-eastern shore of this poition of the lake wherever any outcrops of
rock occur, the banks shelving gently, as a rule, towards the lake with a
gravel or shingle beach along the water's margin.

To the south-west the breccia-conglomerate extends to Rabbit
Point, as well as along the east shore of North-west Bay for some dis-
tance north of Ptabbit Point. The various exposures of this con-
glomerate show no special features worthy of mention in this place.

Rabbit Point. Rabbit Point is a narrow projection that extends into the lake
from the north side of the junction between the main lake and North-
west Bay, a little over six miles from Rabbit Chute. The rock
composing it is the prevailing breccia-conglomerate, but, as in most
cases it is exceedingly difficult if not impossible to determine any lines
of stratification, and the cleavage or foliation which is the most obvious

]

THE MATABITCIIOUAN RIVER.

235 I

and only distinct structural feature present, has a strike of N. 15° E.,
and a dip S. 75° E. < 80.°

There are two small islands about the centre of the lake a short dis- Rocks ex loosed
tance to the west and north-west of Rabbit Point. The larger ""
and more northerly of these is composed of dark grfenish-gray
breccia-conglomerate, the matrix of which has a distinct slaty
cleavage. The pebbles and boulders are composed chiefly of red and
gray granite, and sometimes of reddish-gray gneiss. The inclusions
vary in size from the smallest pebbles to boulders two feet and ovor
in diameter. Besides these composite fragments there are a great
many angular pieces of felspar, which, where they are abundant,
give the rock a pseudo-porphyritic appearance. ]\Iost of tlie f "agments
are composed of a deep Hesh-red granitite, showing a preponderance of
red felspar with a less quantity of gray translucent quartz, and a
trifling amount of green chlorite resulting from the decomposition
of biocite. Next in abundance is a reddish-gray granite somewhat
more basic in composition than the last, while in certain instances
occasional rounded fragments of a distinctly foliated reddish-gray
gneiss were noticed. Besides these there are fragments that seem
to be referable to some of the finer and more compact slaty greywackes
of the Huronian.

In addition to this distinctly clastic material, some granite inclusions Inclv.i^idiis of
were seen with an irregular though lenticular outline, pegmatitic in ''*^'"''
structure and origin. Such patches or areas were sometimes six and even
eight feet in length, which coincides with the direction of the foliation
of the inclosing rock. The strike of the foliation, which is distinct, is
N. G E., with an almost vertical attitude. The smallest of these islands
is composed of a very similar rock, but more massive in structure.
Around the included masses, especially the larger ones of granite, the
rock has an apparent flow-structure, with lines conforming as closely as
possible with the outline of the included fragments. The whole rock-
mass has very evidently been subjected to intense pressure, which has
completely destroyed any bedded structure which may have originally
existed and replaced it by a more or less perfect jointed structure.

Opposite these islands, and forming the eastern shore of the lake, is CoiiKlonRi-
the same greenish-gray breccia-conglomerate, with a foliation striking shoif.
N. 8' E., and a dip to the east varying from CO" to nearly ver-
tical. To the south, as the mass of dial)ase or gabbro is approached,
the breccia becomes much more contorted and broken up. The
included fragments are flattened and rendered irregular in outline,
and the whole mass exhibits abundant signs of pressure and alteration.

V <

■ f

!
1

Contiict with
diabasf.

i i.

I >

H.:'.

236 I

NIPISSIXG AND TKMISCAMING REGION.

Contact t)f
gabbi'o and
quartzito.

At the immediate contact, the conglomerate does not contain many
fragments, and the finer slaty matrix is sometimes alone represented ;
but a short distance away the fragments are so abundant that there is
very little of the finer interstitial material. The junction between the
two rocks is situated a little over a mile and a half south of Rabbit
Point. It is very sharply deiined, and the slaty rock along the line of
donnircation is much broken up and jointed, although the cleavage planes
conform in a rude way v ith the line of outcrop of the greenstone. The
slate is likewise much hardened, as a result of the intrusion, and breaks
with a splintery fracture. The greenstone, which is essentially similar
to most of these basic masses, is doubtless a diabase, possessing a dark
greenish-gray colour and of medium texture. In places it has a
decided reddish tinge, owing to the felspar being stained with hydrous
oxide of iron. This greenstone contains a considerable body of
chloritic and epidotic schist, which may have resulted from the
shearing of a portion of the eruptive itself, or may represent an
extremely altered foi'm of the finer matter of the breccia-conglomerate
caught up and embedded in it.

Towards the end of the outcrop, which altogether occupies scarcely
a quarter of a mile of shore-line, the rock is of a prevailing gray
colour, and much coarser and gabbro-like in structure. Southwards, it
gives place, at the end of a small bay, to a greenish-gray felspathic
quartzite associated with some very vitreous tlesh-red quartzite. In
general, near the contact, these rocks have a north-and-south trend,
but about an eighth of a mile to the south-east the greenish-gray
greywacke was seen apparently striking N. 23' W. and dipping north-
easterly <G0 , but it is improbable that the planes represent true
bedding.

(Jranitic rocks The mass of greenstone described above seems to be closely con-
Lake" nected genetically with the large mass of granite and similar basic rock,
portions of the former occasionally being exposed along the southern
and western shores of Reuben Lake to the west. By far the greater
portion, however, of the shores of Reuben Lake, show outcrops of the
breccia-conglomerate, full of granitic and other inclusions and fragments
and much hardened and altered. It seems probable, that, not only is
the large nuiss of granitic iind other eruptive rock in close proximity
to the west, but also that at no very great depth beneath similar rocks
prevail. The southern and eastern shores of the south-western extre-
mity of South-west Bay, are composed of the breccia-conglomerate with
a decided slaty or schistose structure. On the south shore, the direc-
tion of foliation varies from S. 28° W. to S. 38° W. and the dip south-

THE MATABITCHOUAN RIVEK.

23 7

east < 65° to 70°. The rock, although of a prevailing light greenish-grey
colour, frequently presents pearly-green cleavage-planes, due to the
development of sericite. In this schistose matrix arc embedded pebb-
les and fragments composed chiefly of the red granite.

Two streams enter the small bay forming the south-western end of Streams
South-west Bay. Both of these small streams come from the west, tlu' Snutliwcst
more northerly forming the outlet of Reuben Lake, flows down steeply ^''^y-
over angular and detached blocks (»f slate. The other larger and more
important stream comes in about ;in eighth of a mile from the foot and
drains many small lakes situated to the west and north-west.

The north-western and western shoies of this small Ijay are occupied Rocks df this
by the greenish-yray slaty greywackc and breccia-ci-nglomerate, and at ^"^""'>-
one place near the stream from Reuben Lake, massive and jointed slaty
fels{)athic sandstone forms high perpendicular clilFs. These rocks ex
tend for a little over a quarter of a mile along the shore from the
mouth of this stream, where tlioy ai'e interrupted by an irruptive mass
composed of a greenish-yellow and llesh-red granite-gneiss in alternat-
ing layers. Near the contact the granitic inclusions in the breccia- Contact with
conglomerate become more irregular in outline, and many of them evi- t"^'^"* **•
dently represent dyke-like apophyses of an originally plastic mass
which have been injected through the various cracks and fissures in
the slaty rock,

This gneiss is of medium textuie, and the foliation, which is very fiuu inter of
distinct, is caused by the parallel arrangement of flesh- led and green- ' "' i-'"'^''^''"''^-
ish-yellow bands in alternating sequence. The microscope shows the
rock to be composed chiefly of orthoclase, plagioclase, quartz, chlorite,
(representing the biotite originally present) and epidote with smaller
quantities of sphene, apatite and secondary calcite. In this gneiss
the reddish bands owe their colour to the predominance of felspar
stained by iron-oxide, while the yellowish-green portions represent
bands in which the felspar has undergone extensive saussuritization.
The strike of the foliation is S. 58' W. and tho dip N. 32' W. < 70.

The gneiss occupies the shore southward as far as the stream, which Extent of tlie
comes from the west, a distance of a little over an eighth of a mile. It K»eis.seH.
evidently represents an extension of the much larger mass of similar
rocks exposed in the region to the south and south-west. A mass of
the slate-conglomerate was seen included in this gneissic rock with
granitic intrusions of irregular outline traversing it in various direc-
tions. This mass does not extend further, for the eastern shore shows
continuous exposures of a very fissile and altered grey wacke-slate. This Slaty rockn.
slaty rock was noticed in several places to contain fragments of granite

!l ■ i

M , !

i»» f.

238 I

NIPISSIXC; AND TEMISCAMIN(; RKCION.

Rocks of
North-woat
Bay of Rabbit
Lake.

Diabase.

ViH'kS

Clastic vi
north of K;il)-
bit Point.

and felspar, while at other places they are rare. The rock has evi-
dently been siil)jected to somewhat extensive alteration and deforma-
tion, the exposed edges showing the characteristic wrinkled surface
of slaty rocks which have been exposed to great pressure. The strike of
the foliation varies from N. 20' E. near the foot of the bay to N. 30° E.,
near the north east end. The western shore, south of the mouth of the
small stream near the end of the bay, is likewise composed of similar
slaty rocks, which vary in strike from N. 3° E. to N. 13° E. These evi-
dently belong to a wedge-like strip, which, inland, quickly ends, and to
the south-west is represented only by a number of detached masses
caught up and embedded in the granitoid gneiss exposed on the south-
eastern shores of Eankin and Miller lakes.

The western shore of the North-west Bay of Rabbit Lake, is com-
posed of the prevailing breccia-conglomerate, but generally so massive
that no distinct .stratification can be made out, although usually the
rock seems to strike with the trend of the shore and dip towards
the lake. At one place it forms a cliff named Echo Bluff, over a
hundred and fifty feet in height. A little over a mile and a half north
of Rabbit Point, this slaty rock is repktced by a greenish-gray diabase
which occupies the shore as far as the first narrows, nearly two miles
further to the north-west. Towards each side of the n)ass, the texture
of the diabase is rather fine-graine I, but near the centre it is much
coarser and granitoid in structure, and as a great deal of the felspar
assumes a flesh-red tint, the rock bears a marked macroscopical
resemblance to a basic hornblendic granite. In general, however, the
rock is medium-grained and diabasic in structure and composition.
This basic eruptive extends across the lake to the north-east shore,
where it forms a small patch, the strike of the neighbouring slaty rocks
curving around its line of outcrop. A large patch of the greenish-
banded slates was noticed caught up in this mass of greenstone, still
preserving its bedded structure, with a dip of N. G5° W. < 45'. North
of Rabbit Point, on the east shore of North-west Baj', the breccia-
conglomerate merges gradually upward into a line-grained greenish-
gray felspathic sandstone, interlaminated with much finer-grained
and darker coloured, banded greenish slates, the cleavage striking N.
4° E., with easterly dip < 80°. The dip of the bedding seems to be
to the north-east at a comparatively low angle. This compact green-
ish-gray fine-grained greywacke was examined under the microscope,
and found to consist chiefly of irregular and subangular frag-
ments of quartz, orthoclase and plagioclase embedded in a matrix com-
posed chiefly of chlorite and sericite, which give the prevailing green-
ish tint to the rock. The other minerals noticed were zircon, sphene.

*s^

JW. j

THE MATAniTCHOT'.W RIVEK.

239 I

ilrafinite, accompanied hy leucoxene, tourmaline and large grains of
apatite and epidote. These minerals have evidently suilVred but little
abrasion through the action of water.

To the north of the small area of greenstone exposed on the north- Slaten imrth
east side of this bay, the shore is occupied by greenish slates, banded x,I,.th-we8t''
by the alternation of dark-green and purplish layers which merge into -"^i'"-
one another. Those slates liave ;i strike of S. 42' E., and a dip to the
north-east < 40, Tlie thin section shows the character and composi-
tion of tht>se bands ver}' clearly. Some of the lighter ones exhibit an
augen structure, the lenticules being composed of small angular frag-
ments of ((uartz, with a lesser proportion of felspar. Surrounding and
curving around them are the darker-coloured bands which derive their
colour from the relatively greater abundance of small opaque fragments
of magnetite. The rojk in general may be said to bo composed of a
tine-grair.cd groundmass of felspar, which is now greatly decomposed
into sericite, occurring in the form of minute liglit-yellow-green scales,
chlorite and granules of epidote. Irregular aieas composed of aggre-
gates of chlorite scales, together with small grains of magnetite, are
scattered throughout the section.

At the first narrows, about three miles and a half north of Rabbit I'.anded .slates.
Point, beautifully banded slates of a prevailing pale greenish-gray colour
occur. The colour striping is produced by the occurrence of darker
and almost black folia lines, which doubtless represent a relatively
greater abundance, in these portions of the rock, of grains and dust-like
particles of magnetite ; while the lighter-coloured bands, originally
highly felspathic, contain a considerable quantity of yellowish-green
sericite in minute scales and Hakes, developed at the expense of the
felspar, together with a little chlorite derived from the alteration of
the bisilicate material originally present in the rock. The outcrop is
not far removed from the greenstone mass exposed on the opposite or
south-west shore, and seems to have undergone considerable disturbance
as well as alteration at the time of the intrusion of the greenstone, the
slate dipping to the north-west < 30'.

Beyond this the lake narrows and for about three-quarters of a mile ExtiiMiiity of
has the characters of a stream, including a small rapid. A little above. Ami.
it widens out again into a small lake-like basin, the south-western
shores of which are composed of the massive greenstone.

The portage into White-bear Lake begins at the north-western end Portage to
of this small lake, which is usually considered as a part of Rabbit Lake.
Lake, although not on the same level. The path is scarcely half a
mile in length, and runs on the north side of the stream, which here
trends nearly east-and-west.

I h. ■;

m ^

240 I

NIIM38INO AND TKMISCAMINO UEGION.

Whit.'-btw
liiiko.

iliii

ill! ■

Uocks Clf

.•-.putli-wf.-'nni
IKirt of lake.

( Jrt'Oiislniif or
fliiibase.

Portage to
Hoi^ic Liiki-.

North-fjastcni
part of lake.

Portaf?e fvoui
Wliiic-ltfiu- 'o
Crooked Lukr'.

Rncks of
Crookecl Lake.

Wliite-bear Lake was so called for a former cliief of the Tcmaganii
band of Indians. Ai will be seen by a reference to the map, it has
a very irregular outline, and oidy a little over tlnee miles of the south-
western part is traversed on the cannc-route to Teniaganii Lake, the
greatest portion of the lake lying to the north-east. The principal
bays, making up the larger portion of the whole surface, have a
trend a little east of north, thus ct)inciding with tlie strike of the
clastic rocks exposed on the shores.

Tiiese are connected by shorter intervening stretches, excavated
almost at i-ight angles to the strike of the rocks. The width uf a (piarter
of a mile or a little over is remarkably uniform. Tlie prevailing clastic
rock in the southern and western part of the lake is the breccia-con-
glomerate. The rock is, as a rule, massive and jointed, and the cleavage,
which is the only structure visible, has a strike of abotit north-aiitl south
with a dip to the east <G0°, according in a general way with the line
of outcrop of the greenstone. The greenstone or diabase, as it seems
to be, occupies the whole of the western shore of the southern bay, as
well as the large island near the eastern 'horo about the central part of
the lake. ]talsoforn)s the extremity of Whitel.ear Point and the high
promontory on the south shore separating the eastern from tht; w estei n
portion of the lake. A small mass was likewise noticed on the north-
west shore of the lake about a mile south-east of the inlet from Friday
and Obashking lakes.

On the long portage between White-bear and Bogie Lake, the rock
wherever exposed to the usual breccia-conglomerate, showing a prepon-
derance of granitic fragments inclosed in a dark greenish-gray chloritic
matrix. In the north-eastern part of the lake, the lowest clastic rock
overlying this breccia-conglomerate is a dark greenis ' ^ray fine-grained
greywacke, having in places a somewhat slaty cleavage corresponding
with the bedding. The dip is in gi-neral about S. 75° E. < 25°. This
passes gradually upward, through an interlaminated lighter coloured
felspathic sandstone, into a yellowish-green or greenish-gray quartzose
sandstone or grit, much coarser in texture and more massive in struc-
ture than the greywacke.

A short portage intervenes between the shallow muddy bay forming
the western extremity of White-bear Lake, on the road to Temagami,
and another shallow arm of Crooked Lake or Kinabigo-sminisc
(Snake Island Lake.) The lake has its greatest length from north-west
to south-east of nearly two miles. The rock, wherever exposed, is the
massive breccia-conglomerate, in many places containing numerous peb-
bles and fragments, chiefly of red granite, embedded in a dark-grayish

! !

■ARIOW.

THE MATABITCnOUAN RIVKB.

•241 I

compact felspathic matrix. The strike of the most distinct structural

planes, doubtless those caused by pressure, is S. 47° E. with a dip to

tlie north-east <65°. A portage of less than a quaiter of a

mile separates Crooked Lake from Caribou I^ake, the trail passing Caribou

over a considerable rise composed of the breccia-conglomerate, while J'^'^e to Lake

, _ ., Teina(,'ami.

another portage of nearly the same length intervenes between Caribou

Lake and the small bay which marks the north-eastern extremity of the

north-east arm of Lake Temagami. Caribou Lake, or Sagibanwanapi- Caribou Lake.

kunk is scarce' y three-quarters of a mile long and the rock seen is

the massive breccia-conglomerate, the same rock continuing over the

portage to Lake Temagami. This lake has two outlets, the ordinary

and larger one flowing out of the west end into a small bay to the

south-east of the one entered by the portage, while during times of high

water another small stream flows out of the eastern end into

Crooked Lake.

Three important tributaries or branches of the Matabitchouan River streams enter-
enter the northern part of White-bear Lake. The main branch, W"^^^ Lake
reaches the north-western corner of the main body of the lake about
half a mile north of White-bear Point. This stream takes its rise in
Mountain Lake while many important tributaries enter from the
west, draining the larger portion of the rocky granite plateau situated
between it and the lakes draining towards Lake Temagami. An-
other stream flows into the small bay marking the north-eastern
extremity of W^hite-bear Lake, affording an outlet to a chain of waters
which extends to within a distance of two miles south-west of the Mon-
treal River. The third branch empties into the same bay about three-
quarters of a mile to the south-west of the mouth of the last, draining
several lakes, the largest of which is known as Waibikaiginaising or Rio
Lake.

Ascending the main branch of the Matabitchouan, a portage of nearly Xet Lake,
half a mile separates Net Lake from White-bear Lake, into which it
flows, the trail being to the north-east of the connecting stream. The
lake has a general trend of N. 3G^ W. and the distance from portage
to portage in a straight line is nearly seven miles. The narrows from
which the lake takes its name is situated a little o\er three miles from
the White-bear portage. This contraction is a little over half a mile in
length with an average width of about two hundred feet. South of the
narrows a bay extends from this part to the north-east for about two
miles, at the end afl^ording an entrance to a stream that drains a series
of lakes to the east and north-east.

242 I

NIPISHINO AND TEMISCAMINO HEfilOX.

( ■,:

Stroams enter
ing Ttiie\ inj,'-
bear Luke.

Rocks wen on
Net Lalce.

To the north-west of the narrows, n bay extends to the nouth-weat
for about a mile and a half. A comparatively large sheet of water,
known to the Indians as Kanichee-kinikisink Lake, lies to the north-
west of this bay, int3 which it empties by two outlets, situated
about a mile from one another. The northern portion of the lake,
towards the inlet, is comparatively narrow, never, as a* rule, exceeding
a quarter of a mile in breadth, and frequently contracted to a quarter
of this distance. The outlet from Thieving-bear Lake discharges at a
point a few chains from the northern extremity of the lake, while tho
stream, from Snare and Mannajigainia lakes, enters this lake nearly a
mile to the south-west of this point.

The rock evposed in the south-eastern end of Net Lake, is a mas-
sive compa«.^ f-ark grr nish-gray felspathic sandstone, associated with
small areas or masses of intrusive greenstone. This is succeeded to the
north-west by a flesh-red granitite of somewhat coarse texture, com-
posed of reddish felspar, grayish translucent quartz, and a sparing (juan-
tity of greenish bisilicate material, which was originally biotite and is
now almost completely altered to chlorite. This rock occupies the whole
of the north-eastern shore in the wide space to the south of the narrows.
It also composes the south-western sliore and the islands with the
exception of about half a mile in the vicinity of the narrows, where
there are outcrops of a coarse dark greenish-gray greenstone. The
•shore-line characterized by the presence of these rocks is fairly bold,
in somewhat marked contrast to those where slaty rocks prevail.
There are I'o outcrops of rocks in the narrows. To the north-west of
the narrows, however, the shores as well as the bay which runs to the
south-west, show many outcrops of a light greenish-gray slaty rock,
■evidently originally a compact greywackt', with an abundant develop-
ment of sericite along the planes of cleavage. These slates or sericite-
schists have a strike in accordance with the general trend of the bay,
which is north-east and south-west.

The south-western shores of Kanichee-kinikisink Lake, are generally
composed of a somewhat similar though more compact slaty grey wacko,
l)ut the north-eastern side and many of the islands exhibit greenstone,
which seems to be a different portion of the same magma, which to the
north and north-east has, for the most part, solidified as a biotite-granite
Northern i>iut or granitite. The shores of the northern portion of Net Lake are com-
of Net Lake, ppggj ^f ^ series of rounded rocky points with intervening marshy or
gra sy bays, the rock everywhere exposed being a flesh-red granitite in
which but little of the ferro-magnesian constituent can be seen. Occa-
sional small patches of greenstone were also noticed, that appeared to
be closely related to the granitite.

Il(ieks of
Kiinieliee-
kinikisink
Lnke.

■ADIOW

]

THE MATABITCHOUAN RIVER.

243 I

Mduiitaiii
Lake.

Portage tc
Tt'in.i^'ani
watt'i'c.

A short stream separates Net Lake from Tliioviiig-bear Lake, with
a small rapid near tlie latter and a much larger one near the former.
Tliieving-bear Lake or Mako-gimodiwi has a very irregular Dutline,
heing completely inclosed by comparatively low rounded hills of the
flesh-red granitito. It has three feeders from the north. The route Tliiivinff Iwar
from Thieving-bear Lake northward to Mountain Lake follows a tain hake,
succession of five small lakes or ponds, the largest of which is only a
little over a quarter of a mile in length, united by shallow streams.
Tlie whole distance is about three miles by the stream and the general
direction nearly north. The valley is as a rule somewhat narrow and
shallow, the hills on either side sometimes rising abruptly from the
water. The rock throughout is the prevailing flesh-red granitite.

Mountain Lake has a general trend of k little north of east, and
is about three miles in length in this direction. The western half of
the lake, out of which the portage goes to Breeches liake, is a long
narrow and shallow bay, and the rocks wherever visible are flesh-red
granitite. The main body of the lake is nearly three-quarters of a mile
wide, while the inclosing rocky shores are everywhere composed of the
massive greenstone. The portage from Mountain Lake, which here
marks the height-of-land between the Matabitchouan and Temajjami
waters, passes over the side of a hill, the highest point on the trail
being 160 feet above Mountain Lake. Breeches Lake or Kawagan-
chigania, is small. It empties into a pond which in turn discharges into
a bay of Annimanipissing Lake. A portage of only thiee chains
separates Breeches Lake from the small pond, while another scarcely
an eighth of a mile brings the traveller to the large and important sheet
of water known as Annima-nipissing Lake.

Ascending the stream flowing into the north-eastern bay of Net Ferguson and
Lake about four and a quarter miles from the White-bear portage, the
channel of the creek is utilized for a little over a quarter of a mile,
when a very short carry is necessary to reach Ferguson Lake. Dun-
can Lake, the next expansion encountered, is practically on the same
level, being separated by about a quarter of a mile of stream with little
cni'ri-n' The shores of both Duncan and Ferguson lakes slope gently

id show no rock. The second portage going from the west end of Petrout Lake .
Duncan Lake at the stream from Petrout Lake is about forty-five chains
iu length, n . runs over hills which are composed chiefly of the flesh-
red i>ranitite. Within a short distance of the east end of the portage,
tl is rock is succeeded by breccia-conglomerate of the usual character,
which outcrops on the 'est shore of Petrout Lake a short distance
north of this portage. Jn the opposite side of the lake, a coarse
16i

ii !"

I ^ i

1 "

ii.j

it ■

1 .

H -

nw '

'j;

It ■

;':

244 I

NIPISSINO AND TEMI8CAMING HEGION.

is !

greenish-gray quartzite-grit may be seen resting directly upon tiie dark
greenish-gray slaty rock. The junction is close to the edge of the
water and is sharp, without any of the customary transition from one
rock to the other. Both rocks dip to the east at a comparatively low
angle. The southern end of Petrout Lake is a shallow muddy bay,
and the portage into Lily Lake is along the boulders in the stream.
Lily Lake . The rock on the west side of Lily Lake is the breccia-conglomerate,
showing the usual fragments of rod granite, while on the east side the
slates, which are above, are themselves overlain by the quartzite-grit
that rises into rather high hills a short distance east c f the lake.

A portage of seven chains separates Peeshabo Lake from Lily Lake
into which it empties. The rock on the northern and south-w^ ern
Rocks seen in shores of the lake is the breccia-conglomerate presenting no unusual
feature. A mass of flesh-red granite, evidently co-extensive with the
one exposed on the south-eastern portion of Net Lake, comes out on the
west shore of the lake, occupying a I'ttle over half a mile of shore-line
and an off-lying island. On Bogie Lake, to the south of Peeshabo
Lake, the prevailing rock is again breccia- conglomerate. A portage of
three chains separate it from Peeshabo Lake. A trail nearly a mile
and a half long runs from the south-western end of Bogie Lake to a
hunting camp on the north shore of White-bear Lake, about half a mile
north-east of the inlet from Net Lake. The rocky ridges over which
it runs are all composed of the greenish-gray breccia-conglomerate.

this vicinity.

Granite Lak

James Lake.

Waibikaigi-
naising Lake.

To the north of Petrout Lake, a portage thirteen chains in length
leads into Granite Lake, about a mile and a half in length, although it
is only about three-quarters of a mile from the portage at the outlet,
to that at the mouth of the inlet on the east side, about half way u])
the lake. A short carry of a little over a quarter of a mile of creek
intervenes before James Lake is reached. Granite Lake, as the name
implies, is completely surrounded by granite, with the exception of small
masses of greenstone on the southern and south-eastern shores. The
shores of the southern part of James Lake show exposures of green-
stone, associated with patches and areas of a dark greenish-gray
felspathic sandstone through which it seems to be intrusive. The
northern end of the lake is all composed of the flesh-red granitite.

The portage from James Lake to Waibikaiginaising Lake, starts from
a point on the east shore of the former, about half a mile north of the
outlet. It is nearly thirty-five chains in length, and comes out on the
west side of a small basin, forming the south-western extremity of
Waibikaiginaising Lake. The outlet of this lake flows to the south
from this basin-like expansion, ultimately reaching White-bear Luke

BARLOW

]

THE MATABITCHOUAN RIVER.

245 I

about three-quarters of a milb south-west of its no.'th-eastern extremity.
Waibikaiginasing c. Ileb Lake is a little over six miles in length, and
has, in general, a trend of a little west of north. About half a mile Narrows,
from t! e northern end, a boulder obstruction, doubtless of niorainic
origin, runs almost completely across the lake at right angles to its
general direction, leaving only a very narrow channel near the western
side. The western shore of the lake, wherever rock exposures were Rocks seen,
seen, is underlain by the breccia-conglomerate presenting the usual
dark greenish-gray matrix with embedded fragments and pebbles of
eruptive material. The eastern shores of the southern half of the lake
show rather continuous exposures of the well banded greenish, com-
pact greywacke-slates, upon which is superimposed the coarse yellowish-
green quartzite-grit, both rocks dipping to the east <2i)'. Both
shores of the northern part of the lake are composed of tlie quartzite"
grit as far as the inlet from Johnny Lake.

The portage into Johnny Lake is nearly eighteen chains long and
runs to the north-east of the creek connecting the two lakes. Here a
mass of greenish-gray diabase intersects the quartzite, rising into some-
what high and precipitous clilTs. This belt of diabase is about half a
mile in width and is evidently an extension eastward of the huge mass
exposed on the shores of Annima-nipissing and Mountain lakes. The
shores and islands of the northern part of Johnn}' Lake are composed Johnny Lake
of the massive and compact breccia and conglomerate, much jointed and
broken and filled with very numerous pebbles and fragments of various
eruptive rocks.

The stream from Clill' Lake empties into Waibikaiginaising Lake at Cliff Lake,
a small indentation of its eastern side, a little over two miles from the
south end. The portage is about thirtj'' chains in length and runs a
short distance north of the stream. The canoe-route utilizes only the
northei'n part of Clitf Lake, coming in at the north-west corner and
going out at the end of the small bay running to the northeast. The
lake itself is about a mile and a quarter in length and has a general
trend a little west of north. The j'ellowish-green quartzite-grit rises
into high hills on either side of the lake, especially towards the east,
where liigh precipices mark the western faces of hills that rise to an
elevation of from 400 feet to 500 feet above the lake. These hills
present less abrupt though still steep slopes on their eastern side to the
west of Friday Lake. The strike of these greenish quartzites runs from
N. 25° W. in the southern part of the lake to nearly north at tho

northern extremity, while the dip is to the east < 20 to 25 . The
portage from Cliff Lake to Sumnn't Lake follows up a steep gully,
between high ridges of quartzite to the south and others of diabase to

m !

246 I

NIPISSINO AND TEMISCAMING REGION.

' I

the north. The highest point on the trail is 190 feet above Cliff Lake
Summit Lake, and is only six chains west of Summit Lake, while the fall towards the
latter is seventy feet. The lake itself is only a small pond about a
quarter of a mile in length, the outlet flowing from the north-east comes
into a beaver-meadow and thence eastwards to Friday Lake. The
north-vyest shore of Summit Lake is composed of diabase, an extension
in this direction of the band crossing the foot of Johnny Lake, while
the rest of the shore-line shows outcrops of the greenish quartzite. The
next portage runs from the north-east end of Summit Lake to a beaver
marsh, along the eastern margin of which the path runs for some dis-
Friday Lake, tance, when it turns eastward towards Friday Lake. Friday Lake is
completely inclosed by hills of coarse sea-green felspathic sandstone
or quartzite-grit. The lake has a general direction of a little west of
north and is four miles in length, with an average width of a quarter
of a mile. A trail a little over half a mile in length, runs from a small
bay on the east side of the lake, about a mile from the north end, to a
Wilson Lake, small expanse of water that we callsd Wilson Lake and which has
the distinction of being the highest lake of which we have a record
throughout the entire area of the present map-sheet, being about 1177
feet above the sea.

Prudhomme
Lake.

Stream from
Friday tu
White-bear
Lake.

To the north-west of Friday Lake, a short portage runs to Prudhomme
Lake, the southern part of which is extremely shallow and is inclosed
by the greenish quartzite, but the narrows beyond show outcrops of
diabase which appears to belong to a belt over an eighth of a mile in
width, forming a continuation in this direction of the mass exposed to
the north-west of Summit Lake. North-westward it runs toward the
large mass which characterizes the district on either side of the
Montreal River in the vicinity of Horner Chute, with which it seems
to be continuous. The south-western shores of the northern part of
PrudhoniTne Lake show outcrops of the greenish quartzite striking
N. 25° W. and dipping S. 65° W. < 36^ while on the opposite side
the underlying slates dip S. 70' W. < 35°.

Between Friday and White-bear lakes the distance in a straight line
is about six miles and a half, and the valley occupied by the connecting
stream and lakes shows a gradual bending around from a little east of
south to south-west. The river shows alternating deep stretches, some
of them through extensive beaver-meadows, connected by narrow rocky
or bouldary spaces which require to be portaged. Five portages at least
have to be made before reaching the small laku crossed by Nivens meri-
dian line, to avoid these rough pieces of stream. The streams utilized
for about three-quarters of a mile below this small lake where a port-

n^-

]

MACDONALD CKEEK.

247 I

age over half a mile in length is made to avoid the rough and obstructed
river. A trail a little over half a mile long, runs from the foot of this Portage to
portage to Bear Lake to the east of this point. Below this portage the *"^^ ^ ^'
stream meanders with a comparatively deep though crooked channel, for
a distance of nearly a mile, when a short portage is made on the north-
east side of the stream into Obashkong Lake. This lake is about two
miles in length.

Bear Lake, which flows into the Matabitchouan River below Bear Lake.
Rabbit Chute, has a general trend of nearly north-and-south, and
is a little over six miles in length. It rarely measures a quar-
ter of a mile in width. The shores are everywhere composed of
greenish quartzite with some associated intrusive greenstone at the
southern end. There are two outlets, both of which, however, unite in
a small lake to the south. The stream is rarely travelled and the country
on either side is exceedingly rough and uneven. Three small lake-like
expansions intervene between Bear Lake and the Matabitchouan, united
by rough rocky and usually rapid channels. The slate which underlies
the quartzite is not met with till the immediate vicinity of the Mata-
bitchouan River is reached.

if .. .

Macdonald Creek.

The rocks seen along this stream are particularly interesting and Macdonald
throw considerable light on the structural relations existing between
the Liurentian and Huronian. The stream has never been much used
as a canoe-route, and therefore need not be described at length. It
consists of a series of lakes united by shallow rocky or bouldery chan-
nels, which necessitate frequent portages. From the outlet at the
north-east corner of the Fourth Bass Lake on the Matabitchouan River
to Moxara Lake, it occupies a gently curving valley with a general
southerly direction, but the extension of this depression southward
meets rising land which forms a watershed in this direction. The
upper portion of the stream from Moxam to Ross Lake occupies a val-
ley trending almost north-west. Ross Lake, marking the head-waters,
is only a couple of feet lower than Rabbit Lake, a decided hollow con-
necting the two lakes, and during times of freshet a certain amount of
the water of Rabbit Lake escapes into Ross Lake. The first three ex-
pansions at the head of this stream, viz : Ross, Burwash and Moxam
lakes, differ little in level, and the short stream connecting them
exhi))its very little current. From Moxam Lake, however, down to
the mouth, the fall is seventy feet, most of which occurs between
Cooper Lake and the Matabitchouan, this distance of a little over half
a mile showing a fall of fifty feet.

I' i

1 '

ill!! i

24f

NIPIS8ING AND TEMISCAMIlNG REGION.

Ross Lake. The shores of Ross Lake are composed of a coarse red granitoid-

gneiss, evidently by its composition a granitite. Some portions are
more basic in composition and darker in colour where the biotite has
segregated during its consolidation, and these patches or areas show
a very distinct foliation. In some outcrops the rock is porphy.in'c
and the phenocrysts of flesh-red felspar are developed in a finer grained
felspathic groundmass showing streaks of yellowish-green epidote. At
one point on the west shore, a mass of fine-grained greenstone was seen
associated with the granite in such a way that both had apparently
solidified from the same magma, differing only in their rate of cooling.
The gneissic rock is certainly newer than the greenstone, irregular
dyke-like masses of the former penetrating and ramifying through the
the latter.

Conglomerate. The point on the south-eastern shore of this lake towards the outlet
is occupied by the prevailing breccia-conglomerate holding pebbles
chiefly of reddish and reddish-gray granite. These inclusions vary
greatly in size, some being as much as three feet across. Occasional
fragments are quite angular in outline, some are subangular, while the
majority have been more or less perfectly rounded. The contact
between this comparatively small area of clastic rock and the granitite-
gneiss in \vhich it is doutless embedded was not seen, although only ;i
short distance intervened between the exposures of the two rocks. The
Fig. 4. grerter portion of the small island

in the southern part of the lake is
composed of coarse reddish grani-
tite-gneiss. The island runs in a
north-east and south-west direction
and is about three chains in length.
Its north-eastern point is composed
of the breccia-conglomerate, full of
small pebbles as well as angular
fragments, chiefly of red and gray
granite. The contact between the
two rocks is sharp and jagged and
reentering angles filled with the material of one rock penetrate the
substance of the other.

Contact with
granite.

Scale 40 ft. inch.

Sketch showix(; thk link of junction

at nohtiikast i'oint ol' small

lslani) in bass laivk.

Rocks of I'.ur- The rock near the north-west end of Burwash Lake is, as a rule, well
wash Lake. foliated and of a deep flesh-red colour, the strike being N. 19'' E. and
the dip north-west at a high angle. Some of the gneiss is very mas-
sive and granitoid, in places porphyritic, the phenocrysts of felspar
being very sharply outlined in a dark-greenish chloritic matrix. Tliis

ii'ii

•]

MACDONALD CREEK.

249 I

rock seems to be the prevailing flesh-red granitite-gneiss, the biotite
originally present being decomposed to chlorite. Similar rock is pre-
sent on the north-west shore of Moxani Lake, striking N. 29° E. and
dipping south-easterly < 60°.

On the south-east side of Moxani Lake, in the southern part, and also Moxam Lake.
in the bay running to the south-east, the gneiss is not only very dis-
tinctly foliated, but well lamianted. It is the usual interlamination
of the reddish and grayish granitite, presenting the common alterna-
tion of lighter and darker coloured bands. The strike is N. 48' E.,
and the dip south-east < 53°.

The gneissic rocks in the vicinity of the narrows in the north-eastern cineissic rocks
part of the lake, show a gradual curvinsf around in strike from N. 4° W. "' north-cast-
at the southern end to N. 40" E. a little to the north of this contrac- Moxam Lake,
tion, while the angle of inclination varies from 45' to 60\ At one
point on the north-west shore, nearly three-ciuartersof a mile from the
outlet, the granitite-gneiss is of a deep tlesh-red colour weathering on
exposure to a brick-red. It is massive, distinctly foliated, but much
affected by jointing, so that it is exceedingly difficult to obtain a hand
specimen. Small patches of a dark -green ohloritic slate are embedded
in this rock, running for the most part with the foliation. The slate is
evidently much altered and full of shearing planes, which are
abundantly coated with the usual greenish products of alteration. This
clastic rock contains small lenticular granitite dykes, besides some ill-
detined areas of a similar rock somewhat coarser in texture, that doubt-
less represents squeezed and stretched pebbles and fragments. The hand
specimen from which the thin section examined was taken, shows a
dark -green slaty rock penetrated by tongues or dykes of a dark-red
felsite. Under the microscope, the dark-green portion is seen to be a Lithcilogical
typical clastic rock with subangular and rounded fragments of ortho- '^'''•"''I'^ti'r.
clase, plagioclase and (juartz embedded in a finer grained groundmass
composed chiefly of epidote and chlorite, which have doubtless resulted
from the mutual reaction of the felspar and bisilicates originally pre-
sent. Sphene in irregular grains, and some pyi'ite, were noted
scattered through the section. The little tongues or dykes of felsite
are seen to be composed of orthoclase and quartz chieHy, together with
some plagioclase. The minerals are much bent, cracked and broken,
and have been recemented by chlorite and epidote. The whole rock
has been profoundly sheared and has evidently been derived from a
line-grained greywacke formed from the degradation of a granite, this
rock being subsetiuently penetrated by the fine-grained felsite dykes.
These dykes are all intensely shattered, and the felspar affords beauti-

1! f%

m
f

I '! fl'!

i'i;| I

250 I

NIPISSING AND TEMISCAMING REGION.

Rocks on

eawtern whore
of Moxiuii
Lake.

h (

■;.^ :

i'v

ful examples of twinning striations resulting from pressure. The
cracks are filled with sericite, chlorite and epidote.

On the shore south-east of the island in the northern part of Moxam
Lake, the gneiss is very evenly foliated by the alternating sequence of
massive red felspathic layers, which in themselves show marked paral-
lelism, and dark-green chloritic bands, the whole dipping S. 47° E. < 75".
A few chains to the north-east, the ordinary grayish granitite-gneiss
with very even foliation dips S. < 40' E. 40°. At a point on the east
side of the lake a little over an eighth of a mile from the outlet, there
is a dark-green distinctly bedded rock (greywacke) associated and inter-
foliated with bands and irregular patches of the massive reddish
granitite-gneiss intrusive through it. The rock resembles very closely
a highly altered felspathic sandstone, when broken phenocrysts of
felspar were noticed embedded in the grayish groundmass. The strike
of the foliation is N. ] 3' W. and dip N. 77° E. 70°.
Slaty rocks on ^'^ *^® opposite side of the lake also the dark-red massive granitite-
nortage from gneiss contain a good deal of the highly altered greenish-gray slaty

Moxani Lake. i»,i loi • ir-^i

rock. At the lower end or the portage going north from Moxam
Lake, the usual reddish granitite-gneiss occurs, striking N. 30° W., and
dipping east < 50°. Apparently caught up in the mass of this gneiss
are some patches of a dark-gray slaty rock, very much hardened and
altered and beautifully banded by the occurence of layers rich in yel-
lowish-green epidote. To the north of this, almost in the bed of the
stream, are outcrops of similar gneiss containing many dark-greenish
bands composed chiefly of chlorite and epidote. They doubtless repre-
sent portions of highly altered clastic material and associated with
these are some larger irregular patches of undoubted felspathic sand-
stone. These smaller interfoliated bands have evidently undergone
extensive recrystallization, thus masking their original structure, but
this stratified appearance is in marked contrast to the intrusive aspect
of the granitite-gneiss. The foliation, produced essentially by pressure,
has a strike of N. 2° W., and a dip easterly < 65°. A little north of
the mouth of this creek, outcrops of the massive red granitite-gneiss
contain squeezed fragments of clastic matexial often of very irregular
outline, the strike of the whole exposure being N. 21° E.

Small lakes ^'^ ^^^ ®^^*' ^^^'^ °^ ^^^^ small lake below Moxam Lake, a rock com-

below Moxam posed of alternating folia of red and dark-green material was seen
striking N. 2° W., and dipping to the east at a high angle. A similar
rock outcrops at the southern end of Glasford Lake, the strike being
N. 9° W., and the dip towards the east < 60°. The hand specimen
examined showed a foliated rock consisting of a fine-grained chloritic
groundmass of a dark-green colour, through which runs irregular wavy
tongues of a bright red, fine-grained felsitic-looking rock. In its micro-

MACDONALD CREEK.

251 I

scopic character it bears a marked resemblance to the rock occurring
on the west shore of Moxam Lake, but in tlie case of the chlorite which
is abundantly developed througiiout it, its origin is plainly seen to be
from hornblende, cores of this mineral occurring surrounded by the
chlorite. The felspar is very turbid and is stained throughout by oxides
of iron ; a bright yellow, strongly pleochroic epidote is very abundant
in the section.

The southern part of Glasford Lake is occupied by the massive red ( lueissic grau-
gneissic granite which seems to be composed chiefly of flesh-red felspi'r t.,i(f,,f "j'k".'"
and greenish chlorite or hoi nblende, or perhaps both. The strike f"''<I Lake,
curves around from north to north-east with an easterly to south-
easterly dip 45" to < 60'. This is followed by a compact grayish
slaty rock wiv.h granite inclusions, some of which are pebble-like in
outline and appearance, while others evidently represent approximately
parallel small lenticular intrusive dykes of the neighbouring granitic
rock. This characterizes the shore for nearly a quarter of a mile, and
may represent a tongue or extension of the main mass of similar
Huronian strata to the south-west.

To the northward it may be continuous with an outcrop of breccia-
conglomerate, that occurs on the west shore of Cooper Lake, near its
southern end. The northern part of Glasford Lake is occupied by Granitite-
massive red granitite-gneiss, with which is associated some greenstone, |"j"rt?iein iiart
such areas seemingly representing the primary or first formed secre- "f ^^l-'^^'fo" '
tions from the same magma the cooling of which produced the associated
granitite-gneiss. From this to the second little expansion below Glas-
ford Lake gneiss is the prevailing rock, the strike being N. 19° E.
At one point in the narrows this gneiss contains bands and small irreg-
ular inclusions of a dark-green hornblendic rock. The inlet into
Cooper or Macdonald Lake is occupied by a massive red and reddish-
green, often porphyritic, granitite-gneiss, striking N. 3' E and N. 11°
E,, and dipping to the east at high angles.

The shores of Cooper Lake are occupied chiefly by a flesh-red Sluii-cs of
granitite-gneiss, in some cases poiphyritic, weathering grayish, especi" ""•''' ** '^•
ally when burnt over. The foliation, which is not very apparent in
places, is sometimes brought out more strongly by the more or less
parallel alignment of certain ill-defined patches of more bjisic material.
The rock is composed essentially of flesh-red felspar, chiefly orthoclase,
more or less grayish quartz, this latter material being often present in
vein-like streaks and patches, evidently pegmatitic both in origin and
structure. The little ferro-magnesian material present is apparently
biotite, which has undergone somewhat advanced chloritization. This
is associated with a massive medium-textured greenstone, the irrup-
tions of the two rocks evidently l)eing very closely synchronous. The

W''ni. I

: ■;»■■!

|i:'l

;il, i

F^r^

I'recciiicoii-
gloiiicrati' oil
went short'.

Slate inter-
viiptwl l>y
gniiiite.

Foliation of
rocks at outlet
of Cooper
Lake.

252 I

NIPISSING AND TEMISCAMING REGION.

Stream sepa-
rating Coojier
Lake from
Matalnt-
chouan River.

prevniling strike of the foliation, wherever apparent, is from north-east
to south-west. On the west shore of the lake, south of the narrows,
a patch of the dark greeniah-gray breccia-conglomerate comes in,
apparently forming a huge mass caught up during the intrusion of the
granite. It contains the usual pebble-like and other forms of granitic
material, while the matrix in which these are contained has the cus-
tomary dark greenish-gray colour. This rock occupies the shore for
about an eighth of a mile. The contact between this clastic and the
red granitite-gneiss to the north is irregular and ill defined, irregular
dyke-like forms and patches of the latter penetrating the mass of the
slate. Tiie bedding of the slaty rock abuts on the dim foliation of the
gneis.s, the slate striking N.N.W., while the direction of the foliation
of the granitite-gneiss is south-west.

This patch of slate is interruptea to the south by a red, very fel-
spatliic, granite, which continues along the shore for about six chains,
when it in turn gives place to the dark -greenish slaty rock, similar to
the mass already described, which occupies this side of the lake to its
southern extremity, where the low grouml conceals the rock beneath.
These masses may either represent detached portions of tlie clastic
Huronian strata caught up and floated off during the intrusion of the
association granitite, of whose irruptive character there cannot be a
doubt ; or, on the other hand, they may belong to a band or tongue
co-extensive with the main mass of similar elastics to the south-east,
but whose continuity at the surface is broken, or concealed by the
dense forest growth. The island in the narrows of this lake, as well
as the west end of the comparatively large island to the north, is com-
posed of a greenish-gray green-stone or diabase. At the outlet of
Cooper Lake, the foliation of tlie prevailing granitite-gneiss is
marked by the parallel disposition of plates and aggregated patches
of chloritized biotite. It is sometimes rather obscure, and the rock
is very massivo and granitic in character. The strike is N. 3^ E.

Embedded in this gneiss and crossing its folia-
tion is a rudely rectangular mass of a grayish
slaty greywacke. The mass is about two feet
wide by about fifteen feet in length, the direc-
tion of its longer diameter being about north-
east, while the foliation of the gneiss is only a
few decrees east of north.

The rough and bouldery stream which separ-
ates Cooper Lake from the Matabitchouan
River, shows outcrops of the massive reddish
gneiss, the strike apparently being about N. 1 3°

Fig. G.

'•]

OTTERTAIL CREEK.

253 I

E. At a narrow gorge, through which the stream runs, a patch of
greenish chloritic and epidotic schist was noticed embedded in the
intrusive gneiss. The hand specimen showed a daris-green, rusty-
weathering, compact, foliated chloritic rock, with numerous minute
particles of pyrite scattered through it. The microscope shows it to be
a typical epidotic and chloritic schist in which all traces of the original
structure have been destroyed. It bears a close resemblance to those
described by Dr. F. D. Adams, from the Eastern Townships*, and
consists of a schistose aggregate of felspar, quartz, pale-green chlorite,
epidote and pyrite. The epidote is in granules of varying dimensions,
and also in crystals, which present sharply defined rhombic sections.
It is strongly pleochroic. The chlorite forms pale-green folia, running
through the fine-grained mosaic of quartz an'd felspar forming the
groundmass of the rock. Many of these schists have been proved in SdustM
other regions to have resulted from the shearing of a basic eruptive, T^" "'f ,f^'"
and it is quite possible that this rock has had just such an origin, but, ''/i^ie fiup-
on the c^her hand, taken in conjunction with the other occurrences of *

very similar, though perhaps less altered patches of stratified material
just described as having been caught up in the gneiss, it probably
represents a completely recrystallized basic greywacke-slate.

Between this point and the Matabitchouan there is only another rock
exposure consisting of the breccia-conglomerate, situated on the west
side of the small bay into which Macdonald Creek discharges, and
about thirty chains to the south-east of the main channel of the river.
The junction, therefore, between the granitite-gneiss, here constituting
the Laurentian, and the slaty breccias of the Huronian may be put
down with toorable accuracy as running across the south-eastern end
of this small bay.

Otteutail Creek.

Ottertail Creek (Nikig-wui-no-wui-sipi) rises in a number of small otteitail
streams, draining the extensive swamps that occupy the greater portion (^''f'"'^''
of the north-western corner of the township of Hammell as well as
nearly the whole of the timber limit 21 E. situated to the north of this
township. The main branch of the creek may, however, be stated to
take its rise in a small swampy lake, situated in the fifth concession of
the township of Hammell on the line between lots 8 and 9. The dis-
tance from its mouth, nearly four miles north of the Opimika Narrows
on Lake Temiscaming, to this small lake, is about twenty miles in a
straight line bearing S. 50° W., but following the bends of the stream

■•'!t)

i'\ [\-

•Report of Progresij, Geol. Surv. Can., 1880-82.

Sf hi

11^

, ,,

!| ; 1

I .?!/

lifl i^

ri;

Braiu'li \iscd
as route to
interior.

Portages on
mute itiliiud.

f>rii,'in of
wiiter imli-
catt'd liy
colour.

L;ik<:' at forks
of (Jttei tail.
Creek.

254 I

NIPISSrXG AND TEMISCAMIXG REGION.

this distance is increased to a little over thirty miles. The most impor-
tant branch, however, forming as it does a portion of the route occa-
sionally used by travellers to reach the interior, takes its rise in a
small beaver-pond a short distance north of the northern boundary of
timber limit 12 E. This pond is separated by a portage of only a
quarter of a mile from another small expansion known as Bush Lake,
that flows into the Martin River, about three-quarters of a mile south-
west of the inlet from Mackenzie Lake. The distance from this small
beaver-pond to the mouth, following the course of the stream is
twenty-two miles and a half but in a direct line, bearing !S. 71" W., it
is only a little over sixteen miles

The first portage on the route inland by wa}' of this stream, starts
from Grenier's clearing, a short distance north of the mouth of the
stream and is a little over a mile in length. It runs from the valley
over the high hills, that bordei Lake Temiscaiuing. The upper por-
tion of these hills shows the usual hummocky outline which elsewhere
occurs with extended exposures of the reddish gneiss. This rock is
massive and granitoid in appeai-ance, but distinctly foliated, the strike
being to the northeast while the dip is to the north-west < G5°. The
highest point on this portage is 3(15 feet above low water on Lake
Temiscaming, while the creek reached by the west end of the portage
is 180 feet above the same datum. The descent, therefore, towards the
creek, though less (285) than that towards the lake, is very abrupt and
steep. Four more portages intervene before the lake at the forks is
reached, these showing a combined fall of nearly eight-four feet. The
portages are all on the north-east bank of the river and are short,
the longest being a little over half a mile. These are to overcome
low rapids caused chiefly by bouldery obstructions. Between these
rapids the creek is comparatively deep and about twenty yards in
width, flowing with a gentle current between banks composed of
coarse, yellowish sand. The water is of deep brownish colour, showing ,
its swampy origin. The rock, wherever exposed, is the common granitite.
gneiss, very massive and granitoid in structure, but with distinct

foliation, striking N. 30° E., and dipping to the north-west < 05'.

The main forks, where the north branch joins the main stream, is
about four miles from the month, the creek throughout this distance
having a general course of N. 7G' W. The lake at this fork represents
in reality the last stretch of the north branch before it enters the main
stream. The name Wabamik, by which it is known to the Indians,
refers to the legend that a huge white beaver formerly lived on its
shores. The immediate banks of the lake are for the most part low
and marshy, but two exposures of rock which were noticed resembled

**f''

•]

OTTERTAIL CRERK.

255 I

the massive reddish granitite-gneiss striking N. 35° E., and dip-
ping to tiie south-east < 70\ A few hills rise to the south Hills -.outU
of tlie forks, but at a considerable distance away from the creek,
while the valley of the creek immediately above is wide and level.
To the south-west of the lake, a rather prominent hill rises in
close proximity to the shore, while to the northeast the numerous
rounded rocky ridges of the usual flesh-red granitite-gneias rise from
200 to 250 above White-beaver Lake.

Between the forks and the intersection of the Lake Temiscaming Kl"veii
colonization road, the distance V)y the stream h about eleven and a half
miles. In this distance there are nine poitages, to overcome as many
rapids and chutes. Seven of these are low rapids where the stream is
obstructed by boulders, while two are chutes, the channels being com-
paratively narrow and cut for the most part along the strike of the
foliation of the gneissic rock. The i"t'^"v»^.ilng stretches of quiet water,
between these interruptions to navigation, average nearly a chain in
length, the water being tolerably deep, and the banks on either side
fringed with a dense growth of alder and willow. The stream in many
places pursues a rather tortuous course through the narrow sandy flat,
although some of the more prominent bends reach the solid rock on
either side of the valley.

At the first rapid above the forks, the stream falls about ten feet VWst ivipid
through a gorge excavated in flesh-red granitite-gneiss, well foliated '
and laminated, and striking N. 38" E., while the dip is to the south-
east <45" The gorge or canon runs for the most part with the folia-
tion, but at one place it breaks across the strike of tlie gneissic-rocks.
At the lower end of the third portage, the gneiss is the dark -gray,
ahnost black, variety, which is at once hornblendic and micaceous, and
to which the name quartz-mica-biotite has been applied. It is a glist-
ening evenly foliated gneiss stained in places with iron oxide. The
strike at this place is about north-east, thus corresponding with the
general trend of the stream. Under the microscope, the rock is seen to
be composed of plagioclase, orthoclase, quartz, hornblende and biotite
with sphene, apatite, zircon, pyrite and limonite as accessory minerals.

At the sixth portage, (made to overcome a i-apid which also flows Encks (m
through a rocky gorge cut out along the strike), the rock is dark- .^.'.vfiiUiport-
gray and micaceous, well laminated as well as foliated and striking "d«-
IS!. 22" E. with a dip.to the south-east < 45°. At the seventh portage,
the rock is the fine-grained reddish granitoid variety, doubtless a

granitite-gneiss.

Between the bridge on the

Lake Temiscaming

colonization road and the forks with the main branch above, there are

256 I

NIPISSING AND TEMISCAMING HEGION.

JUiJI

iii

three obstructions in the stream. Two of these are caused by boulders,
but the third, which is internieiliato between the other two, shows a
descent of nearly thirty feet with a portage on the south aide. The
rock at this place is massive and much jointed, and represents the
prevailing red granitite-gneiss. At the third rapid above the bridge,
the rock present is massive, rather fine-grained, reddish in colour and
distinctly gneissic in structure. The thin section under the microscope
shows it to be a granitite-gneiss, composed of orthoclase, plagio-
clase, microcline, quartz, biotite and primary epidote, the orthoclase
being by far the most abundant constituent. The accessory minerals
noted were apatite, zircon and sphene.

Navigation A short distance above the rapid, the surface of the country flattens

beav't'ixhiiiiH^ °^^' "^^^ile the creek itself, for a distance of over two miles, pursues a
tortuous course through an extensive beaver-meadow, and numerous
beaver-dams obstruct navigation. It is expedient to make one long
portage avoiding this portion of the creek and coming out at the south-
east end of Ruth Lake. Ruth Ijake, and the beaver pond beyond,
marking the head of the Ottertail in this direction, are practically on
the same level, and the portage connecting them runs on the south-west
side of the creek. On this portage some birches, over nine inches
in diameter wliich had been felled by beaver, were noticed. The
strike of the rock in Ruth Lake is about south-west. It shows the
usual alternating reddish and grayish bands which, in themselves
foliated, give by their even and parallel disposition, not only a
very marked foliation, but a distinct lamination to the whole mass.
Under the microscope, a specimen obtained from the north-east shore
shows the rock to be of the variety here designated granitite-gneiss.
It is composed of orthoclase, microcline, plagioclase, quartz-biotite and
primary epidote with apatite, zircon, sphene and a little iron ore as
accessory minerals.

Portapp fi-diii From Ruth Lake, a portage a little over a mile and a half in length

Rutli Liikc to rung ^q Fanny Lake, at the head-waters of one of the tributaries of the

r aniiy Lake. ■'

Martin River. The .south-western end of the portage passes over a .some-
what low, though in places rocky tract, grown up with small trees.
There is little soil, and the rock, when exposed, was seen to repi'esent
red and gray banded granitite-gneiss. The last half-mile near the
north-east end of the portage approaching Fanny Lake is over lower
land, very marshy in places.

The portage from the beaver-pond to Bush Lake is about a quarter
of a mile in length, and the barometer showed the latter to be ten feet
lower than the beaver-pond. The shores of Bush Lake are compara-

BARIOW

HAY LAKK TO LAKE TEMAHAMI.

m I

tively high and for the most part rockj-. A hill rises close to the south-
west shore of the lake to n height of aVjijut \nO feet. The rock which,
is frofineiitly soon is a f,Manitite-gneis'<, wt'll foliated, but somewhat
uiassivo and granitoid in structure. The strike is N. -1")° E. and the
(lip southeast <bO\ The portage from Bush Lake to the ]\Iartin
Uiver, into which it empties, shows a fall of about forty feet. The
trail starts from the north-east side of the crook, but crosses over to the
south-west side. It shows evidonco of having been but slightly
u cd. Indeed the whole route inland by way of Ottertail Creek is
hut little known and therefore rarely used, and as the beavers have
hoen nearly all exterminated in the vicinity of its banks, it has been
Init little freijuented of late years for hunting purposes. Occasiimal
licrivcrs, however, still reside along the course of the creek, as abundant
work done quite recently showed.

Kuiitf liy
Ottcrtiiil
Crt'ck little
kiidw 11.

! t|

Bay Lake to Lake TEMAnAMi, nv way ok Axnima-nipissinc;,
Carrying, and Red Squirrel Lakes.

Tliis route commences at a small marshy bay on the south-west side jj'i'itr from
of Bay Lake, about one and three-cpjartor miles south-east of Bay Lake i jik,. "
post. The narrow and crooked, though navigilAc, channel of the small ' '"'''f-''""!
iiilnt that enters tlu' lake at this point, is followed, a short distance, to
tli'^ foot of the portage. The poilage is in reality a winter road, built
\i\ 1891 by Father Paradis to take in supplies from Bay Lake to Tema-
•,'aini, and is a little over one mile and a quarter in length of almost
cmtinuous climbing, reaching Anniina-nij)issing Lake at the extreme
uortli eastern corner. Tiie trail follows up a valloy, which, as the sum-
mit is approached, becomes very nari'ow, the hills of quart/ite-grit on
I'itli'M' side approaching each other very closely, while a talus of angular
liloeks detached from the heights above still further obstructs the
narrow pass. At the summit, a sort of rid de sac occurs, the steep
slojie facing towards Bay Lake, but once this sharp incline of lifreen
feet is surmounted, there is a gradual descent of about ten feet to
Annima-nipissing Lake. This lake is about one hundred and eighty Anniin.a-
feet above Bay Lake or 1073 feet above the sea, while the highest point Ljli^^r'"^
on the portage, only a short distance from Annima-nipissing Lake, is
only i,?n feet higher.

Annima, nipissing or Aminipissing Lake, (the name meaning the
head of the Nipissing waters), runs in a general direction of S. 30° W.
for nearly ten miles. It is separated from McLean Lake, to the south-
west, by a small narrows, containing a rapid, and which although show-
ing a decrease in level of about two feet, is sometimes described as
17

i!^

hfc..&l

nil

■i

(jlIHfill

dcscrii)tion.

Di'.sci'iptidii

of soutliri'U
part .

Ai'kdsp of
]5:i.v Lake
«'xtcii(titi(^ to
Aiiniiiia-
iiipissiug
Lakt'.

Quartzito
altcicil liy
intrusion of
gabbro.

258 1

NIPISSINO AND TKMISCAMING REGION.

forming part of the larger expanse. This important sheet of water is
divided into tliree portions, separated by two narrows. The most
northerly of these .stretches, has a length of four miles and three-
quarters and varies from a quarter of a mile to a mile in width. Tho
central portion is much smaller and presents a much more irregular
outline. One of the bays running to the south-east affords an entrance
to an inlet from Breeches Lake, on the road to Mountain liake, at tlic
head-waters of the main branch of the Matabitchouan River. A some-
what longer arm running a little west of south, approaches very close to
the waters of Mannajigaina Lake, while still another extension, running
to the north-west, receives the small creek from Picken^l Lake, from
which it is separated by a portage only a few chains in length.

The southern part is about three miles and a half in length and is
over half a mile wide. It likewise has an irregular shape, a large bay
running to the north-west for nearly two miles from the noi'thern end
of the stretch. About a mile and a half from the outlet into McLean
Lake a small stream enters, forming the outlet of Whitewater and l^ia-
base lakes. Several soundings were taken in jilaces reported to be
exceedingly deep. One of these places, situated about the middle of
the lake, opposite Crow Rock and a little over a mile from its nortlicrn
end, showed a depth ?i ninety-three feet, while another sound-
ing, taken about the middle of the large open space in the central part of
the lake, gave 100 feet. The water has the clear and limpid char-
acter and light sea-green tint of Temagami, although in point of clear-
ness and purity both of these lakes are excelled by AVhitewater Tiake,
lying to the west of the southern part of Annima-nipissing Lake.

The coarse quartzite-grit or arkose occurring on Bay Lake, extends
to the tract passed over by the portage entering the north end of
Annima-nipissing Lake. It also extends down the eastern shore of
this lake for nearly three-quarters of a mile, when it gives place to a
coarse gabbro that occupies the shore for over a mile further south.
The rock, as here exposed, is rather coarse in texture, and is character-
ized by the presence of reddish felspar, in this respect resembling cer-
tain portions of similar irruptive masses to the north-west of Bay
Lake, as well as at Quinn Point on the east shore of Lake Temisca-
ming. Near the line of junction with the gabbro, the quartzite has
been considerably altered by its intrusion, the alteration consisting
chiefly in a hardening due to the secondary enlargement of the
original quartz grains and the deposition of intersticial silicia. C'n
the west side of the lake, this arkose forms a perpendicular cliff about a
hundred feet in height, known as Crow Rock, and, continuing down

**-y-,

'•J

BAY LAKE TO LAKK TKMAGAMI.

259 I

along this shore occupies the greater part of the southern shore ot the
bay running to the south-west. The large island, as well as the much
smaller one to the north-east, is composed of massive greenstone or
gabbro, but the island lying close to the shore to the south-west of
these is foriued of the slaty grey wacko, underlying the arkose. (-)n the
point to the south-west of the large island, a considerable inlier of
banded slate appears to have been caught up in the mass of tlie green-
stone during its iri'upiion, and the bedding of the slate well marked
by the alternating coiour-bands, shows an inclination N. 50 W. < 15°.

The relative distribution of the greenstone and slaty greywacke, Distrilmtion
the latter being the prevailing clastic rock, is shown on the map. The .j,„^ txrvy-
diabase gabbro forms a series of high hills which are in marked ^^■"'^k'^'-
contrast to the Hat topography characteristic of the areas nnderlain by
the slates. On the west side of the lake this greensto.T: sometimes
forms the shore-line, while elsewhere it is replaced by a strip of
the slaty greywacke only a few chains in width. The clastic rocks in
this poition of the lake have a prevailing dip to north-east or north-
north-east at a low angle, usually less than 10'. The southern and
south-eastern shores of the central portion of the lake show somewhat
extended exposures of greenstone, both gabbro and diabase being
present in the same mass. To the south, these rocks seem to merge
gradually (through a massive grayish or pale-pinkish gneissic granite
well exposed on Mannajigaina Lake), into the mass of desh-red granitite
and granititegneiss, that prevails over such a large area to the south
and south-west. The field relations of these several rock-types, seems I'idil ii'hi-
to furnish considerable proof that all three have originated from the [|"]'^^'|„j\'^."''''
same magma, differing only in their rate and manner of cooling. The i^'"'"' <" igi".
irregular point of land on the north-west side of the lake, between its
northern and central portions as well as the extreme point on the
east side of the narrows, is composed of rather flat-lying slaty strata.
On the west side of the southern stibc h \.,i Annima-nipissing Lake, is a
range of hills composed of irruptfvc Diaterial, chietly a rather coarse-
grained granite.

Closely associated with the last-named rock, is that to which the
name breccia-conglomerate has been applied in this Report. The Bnccia-
matrix is, in general, a dark grayish-green chloritic and epidotic grey- congloiuerate.
wacke, inclosing numerous fragments of various irruptive rocks, those
of Hesh-red granite being the most abundant. These are often quite
angular in outline, occasionally showing re-entering angles, although
usually they possess a more or less perfect rounded outline. These
larger fragments include pieces of flesh-red felspar and grayish quartz

- j
ii

i: 1

260 I

NIPISSINO ANIJ TEMISCAMING REGION.

fraKiiients.

mmni ^

or quartzite, red and reddish-gr<ay granite, fine and medium-textured
Colli] loncnt diabases and sometimes diorites of several species. Occasionally frag-
ments of a greenish slate, apparently identical with some classified as
Huronian, were also noticed. This coarse material is occasionally so
abundant that little of the finer mat -ix is represented, while, elsewhere,
only an occasional pebble or fragment was noticed, the rock passing
upward into a distinctly banded slate, which is usually entirely free
from such inclusions.

Hills cliictly
cif j^'iMiiitc and
(liabasf.

|:i!j!
W

V t

^rn(l.■flf fciiin- from one to the other

atiiiii of rocks

(irolialily

diffciC'iit.

WliircwatLT
Lakr.

The greater portion of these hills is composed of a \'ery pale flesh-
coloured granite, which is associated with and apparently merges into
a greenstone or diabase. One point shows a prevalence of the granite
with bauds and patches of the greenstone scattered through it, while
otluM' outcrops, not very remote, exhibit a preponderance of the green-
stone, with irregular dyke-like forms of granite penetrating it in all
directions. Both granite and greenstone invade the breccia, while
fragments of the latter are caught up in both of these intrusives. Tiie
contact between what is evidently a pyroclastic rock and the igneous
intrusives, is a curious wavy line, which in places can be laid down with
exactitude, while a short distance away there is apparently a comingling
of the two rocks through fusion, that causes a seeming transition

The history of the formation of these several
rocks, would seem to indicat*- that the granite and greenstone repre-
sents difierentiated irruptives, forming the original deep-seated por-
tions of an old centre of volcanic activity, which subsequent erosion
and denudation have exposed at the present surface. The breccia-
conglomerate, on the otlier hand, doubtle.'-s constitutes the lower por-
tion of the associated volcanic breccia, formed by the accuiimlation and
consolidation of portions of the various strata rent asunder during the
progress of the eruption, this resulting pyroclastic material being spread
out upon the bottom of a shallow ocean, where it has become rolled,
sorted, and possibly mixed with ordinary aqueous sediments. The
overlying slates show very little sign of aqueous abrasion, while in their
composition and appearance under the microscope they closely resemble
fine-grained tuffs, representing the consolidation of the first volcanic
ash beds.

Whitewater Lake ( Ivavvabish-kagama) is an irregular sheet of water
running in a general direction of a little north of west for about three
miles. It empties from the west into Annima-nipissing Lake about one
mile and a half north-east of the outlet into McLean Lake. A short
portage, over exposures of breccia-conglomerate, follows to the north
of the discharging creek. A belt of diabase runs from the western

BAY LAKE TO LAKE TEMAGAMI.

261 I

shore of Annima-nipissiag Lake to tlie south of this lake, forming the
points of the small peninsulas near the west end of the lake, and con-
necting with the large mass of similar rock to the west and north.
The elastics associated with this greenstone include the massive, dark
greenish-gray greywacke with or without large inclosed pebbles
and fraguients. Diabase Lake, about a mile in length, is separated Dial )aso Luke,
from AVhitewater ]jake to the south, into which it empties, by a short
portage, and, as its name implies, is completely inclosed by greenstone,
that to the north-west of the lake rises into considerable hills. Gull
Rock Lake is reached by a portage considerably over half a mile in
length fiom the nortli-west end of Pickerel Lake. Tt is so shallow
that the Indians assert that during severe winters it is frozen solid to
the bottom. Its outlet, leaving the north-west angle of the lake flows
into the Montreal River a short distance below Pork Rapid. It is
completely surr junded by low hills of the coarse quart/ite-grit or
arkose.

Lakrs

.■^oiith-ca-t
of Aniiiiiia-
iiipi^^iiiK
Lake.

Mannajigama ^^ ugly-running) Lake and Snake Lake (Nakwaganak)
lie a short distance to the south-east nf the southern part of Annima-
nipissing Lake, the former being reached by a portage about thirty
chains in If^ngth, running from the extremity of a bay on the east side
of Annir . .' issing Lake, about two miles and three-quarter from its
outlet to ^>u i^ean Lake. Tlu' shores and islands of ]\Iannajigaina
Lake, which runs west for about two miles, are composed of a grayish
and pale Hesh-coloured gneissic granite, the foliation, though at times
somewhat indistinct, being nearly alwaj's discernable. Snake Lake,
the lower of these two expansions, is also surrounded by a very similar
intrusive rock, with the exception of the south-eastern corner, where a
comparatively large patch or area of the breccia-conglomerate is exposed.
The immediate shore-line, on this side of the lake, is occupied by a
narrow strip of granite, while, immediately to the south, the breccia-
conglomerate forms a rather high hill, with a dip to the south < 8°.
Tiie contact between the breccia and the granite is at times very shai-p
and distinct, when it exhibits a curved or sinuous line, but at
other times there is a narrow brecciated zone, caused by the invasion
of the breccia by the granite and the inclusion of fragments of the
former in the latter.

The eastern shoi-e of the southern part of Annima-nipissing Lake, is pocksc.n
composed of the dark greenish-grav greywacke-slate, containing frag- ^'|"f'i iii«t-
ments and pebbles of granite and other irruptive rocks. The slaty of .Viiuinia-
■ rocks characterize a band on this shore varying from an eighth to a Ljlk^.']'"'^
quarter of a mile in width, while the south-eastern part of the two small

'4
't
I

' 1

262

NIPISSING AN'D TKMISCAMING REGION.

bays that indent this shore-line, show continuous outcrops of a flesh-red
J,"- issic granite. On the south side of the more nortiierly of these two
indentations, the immediate contact between the granite and the slates
was noticed, the latter rock dipping N. 50' W. <50 , while the folia-
tion of the granite has an inclination S. 87° E. <70 . At the foot of
the more southerly of the two bays, the foliation of the granite-gneiss
has a strike of N. 47" E., and a dip to the north-east <4:5"

McLeaiiLMke. The greater part of the north western shore of McLean Lake, is com-
posed of 1 very much squeezed and altered chloritic grcywacke-slate. This
likewise occupies the points on the south-eastern shore, but the granite-
gneiss ' fops out all along the bottom of the bays as well as along the
.\rcL.';ui Lake sides towards the south and south-east. The portage from McLean
Lako. ' ' '" Lake to Carrying Lake (Kecheonai) is nearly thirty -five chains in
length, and the rock, abundantly expi)sed, is a coarse llesh-red
gneissic granite, the foliation being marked by the parallel disposition
of chloiitized scales of biotite. In composition the rock is a granitite,
being composed chietiy of orthoclase, quartz, biotite, decomposed to
chlorite, with smaller quantities of epidote and sphene. The strike of
the foliation on Carrying Lake is N. 42° E., with a dip to the south-
east. The contact between the granite and the breccia-conglomerate
runs across Carrying Lake near its centre, the clastic rock, having a
strike of N. 72° E., and a dip to the north-west < 00°.

Portage to The portage into Red Squirrel Lake (Atchimo) is over Iialf a mile

['.* Uir^"""" lotig) 'i-'id shows, at the beginning, exposures of breccia-conglomerate.
Outcrops of the same rock are very abundant on Eed iSquirrel Lake,
and on one of the small islands, the granitic and diabasic fragments
and pebbles are so abundant that very little of the dark-greenish
chloritic matrix can be seen. On the south-east side of the lake, this
rock rises into hills about three hundred feet in height, dipping
S. 1 7° E. < 45. To the west and south-west of Ked Scjuirrel Lake,
steep hills of diabase rise to a height of nearly four hundred feet above
it. The portage from Red Squirrel Lake runs to a small marshy
expansion of the Annima-nipissing River, starting from the end of a
small bay on the west side in which is the outlet.

Trail eni.-s- T'he trail is about fifty chains in length, crossing the Annima-

iiig Auniina- Nipissing River or outlet by means of a small-rocky island about a
iu|iissing 1 o J " . . ,

Kivei'. quarter of a mile from the lower end. The rock at this point is the

prevailing breccia-conglomerate containing chietiy granite fragments.

Between Red Squirrel Lake and the crossing of the river, the portage

passes over a sharp and steep esker-like ridge of sand that runs about

north-and-south, corresponding with ti;e direction of ice-flow in this

HARLOW. J S

locality. From t
mile down the str
Ferguson Bay on

SffARP Rock Inl

Nonwakaming
have of late years
they form a consi(
Lakes Temiscamii:
which runs from J
by the Haileybu
Montreal River, is
po.-,t on Bear Tslan
Matahitcliouan Ri
tance is only forty

The first portagi

abiiut a quarter of

(it the stream, wlii(

as a northern outl

angular fragments

having suggested

known. Nonwaka

The first-mentioned

that five portages

directions. These

wards Lake Temii

to the south-west t

west, a long portag'

sion that emptii's i;

fiMin the northern 1

while the other tun

tSliarp Rock portagt

Lake, tlie distance is

a little west of nort

ted close together o

mile from the end o

The largin- part
a direction a littl
approximate a\orag
biys, the sm.iller o;

v.]

SHARP ROCK INLET TO MATTAWAPIKA.

263 I

locality. From tlie foot of the portage it is nearly three-quarters of a
mile down the stream to its mouth on Sandy Inlet at the north end of
Ferguson Bay on Lake Temagami.

SirARP Rock Inlet (Temagami) to Mattawapika (Moxtral IIiver.)

Nonwakaming and Lady Evelyn lakes, which occupy this interval, Xoiiwaknu-
have of late ye.'i!'s become rather well-known topographical features, as Eseh-n hikes.
they form a considerable portion of a favdurite canoe route between
Lakes Temiscaming and Temagami, conunencing at the long portage
which runs from Ilaileybui'v post-othce to Sharp Lake. The distance
by the Haileybury route, following Sharp and .Mud lakes and tlie
Montreal River, is about seventy miles, to the Hudson's Bay Company's
po.-.t on Bear Island in Lake Temagami, \vlule from the mouth of the
Matabitchouan River on Lake Temiscaming ti the same place the dis
tance is only forty-three miles following the canoe channel.

The first portage fron. _Lake Temagami to Nonwakaming Lake, is I'nitnirc ivnm
about a (juarter of a mile in length and is situated on the north-east side 'rtiii;iL,'!iiui to
of the stream, which, during the earlier months of summer, oidy serves ■ ""["/|.'^ ""'
as a northern outlet of Lake Temagami. The trail is strewn with
angular fragments of the subjacent light-green banded slate, this fact
having suggested the name " >Sli.u'p-rock Portiige," by which it is
kiiovvn. Nonwakaming i^ako is sometimes also calk'd Diamond Lake.
The first-mentioned name is of Cliippawa derivation, referring to the fact
that five portages afford an exit from tlie lake in as many di liferent
directions. These include, first one running to the southeast to-
wards Lake Temagami. The western bay afiords a route going
to the south-west towards Wakcmika Lake and anochrir to the north-
west, a long portage connecting the waters of this lake with an expan-
siou that empties into Sucker-gut Lake. The two other trails issue
fr.im the northern bay, one running north-v/est to Sucker-gut Lake,
while the other turns to the north-east into Lady Evelvn L:i.ke. From
Sharp Rock portage to the route affording an entrance to Lady Evelyn
Lake, t!ie distance is three and three tjuarter miles,in a general direction
a little west of north, the portage and the outlet of the lake being situa-
t"d close together on tiie east side of the lak'% about three-(iuarters of a
mile from the end of the long bay that extends :ii this direction.

The larger part of the area of the lake Is an arm running in ji,,jj(^,,.j.|fj,,„ ,,f
a direction a little north of west, for about five miles, with an ><'<>iiwiik;iiii-
approximate average width of half a mile, endinu in two subsidiary
biys, the smaller one running to thi^ north-west, while that to tlie

r.,..-i!^-'m

■Hi

Jlri-iM

264 I

NIPISSING AND TEMISCAMING REOION.

'■^ ■ m

liii! 1

y.'s

Rocks
t'Xlio-^fd

Ti'.eir strike.

yiijiiilii t I

Traiii-iition
friim slates to
arkose.

south-west continues fur nearly two miles fui'ther. The eastern side
of the lake is flat and the ends of the bays are low and marshy, while
the shores aloni,' the west side present the steeply sloping sides of bold
rocky hills that come close to the edge of the water.

The rock exposed on the east shore, is an evenly banded green-
ish slate, the planes (jf cleavage corresponding with those of the bedding:.
This shite occupies the whole of that shore as well as the two
smaller islands close by. In strike, it exhibits a gradual curve from
N. 20' W., in the south-eastern part, to N. 20' E. in the vicinity of the
portage going to Lady Evelyn Lake ; while the angle of dip, always in
a westerly direction changes from 8° in the southern portion to 45'
along the east side near the north end. This rock exhibit a transi-
tion upward through a more massive durk greenish-gray slaty rock,
that occasionally shows the colour-bands so characteristic of the strata
beneath, into a compact greenish felspathic sandstone, which, in turn,
merges above in a rather coarse quartzite-grit or arkose. The gradual
transition is well shown on the two larger islands situated near the
centre of the open space formed by the junction of the several bays.
The arkose occurs in very thick beds, generally well jointed, but so
massive that, usually, it is dilHcult to ascertain its true dip or strike.
As a rule, the rock is of a pale yellowish-green or grayish colour. Tie
fragments usually apparent to the eye, consist of a pale reddish
or grayish felspar with a much larger proportion of grayish or
colourless quartz, embedded in a matrix composted chiefly of minute
scales of yellowish sericite. In places along the north shore of the
western bay, some of the beds are of a distinct flesh-red colour, being
tvith difliculty distinguishable from ordinary granite, from the degrada-
tion of which they have evidently been formed. Under the micro-
scope this phase of the rock is seen to difler from the prevalent green-
ish type, in that the felspathic and quartzite fragments are little
rounded and accompanied by little sericite.

This (^uartzite-grit occupies the shores of the western bay of

wi .:i' n\ bay JsTonwakaming Lake exhibiting a prevailing dip to the east of north-
coiiiposed or ^ o r o r

(|iuirtz;ito-giit. east < 12 to 15'. The Muall bay forming the south-western end of
the lake shows an intricate labyrinth of narrow channels, separated by
small rocky, hummocky or subangular masses of the quartzite-grit, the
brook emptying the litt'e expansion to the south-west through a nar-
row valley of a somewhat similar character. The rocky portage, which
is scarcely a quarter of a mile in length, leads to a little lake whii li
is completely inclosed -by ridges of the arkose. The trail from this
pond to the north-west bay of Wakemika Lake is somewhat longer.

Shorts of
1.
ipose

]

SHARP HOCK INLKT TO MATIAWAPIKA.

•265 I

and passes over ledges of the (juartzite-grit. Wakt'mikii Lake is \V;ik('iiiika
a little over throe niilos in length, and the main portion shows a
Width of over two miles. The north-eastern bay is almost com-
pletely separated from the rest of the lake by two opposing ridges of
sand which leave a very nari'ow intervening channel with a gentle
current. A considerable bay on the western side of the lake
is formed by the projection of a long niirrow point or peninsula fiom
the southern shore. The outlet of the li»<ie is into Obabica Lake, about Outlet into
two miles distant to the south-east, with only two intervening portages. lT,,'""'^
The lake has been excavated for the most part in the massive or upper
part of the prevailing banded slates, that here a dip N. 75' E. <12\
At one place on the south shore this slate is seen to have developed a
perfect cleavage, striking N. 20' W., and dipping west < 80^ These
slates show the usual transition upward, through a narrow belt or
zone of tine-grained greenish felspa,thic sandstone, into the coarse-
grained light grayish-green arkos?, wliose massive beds dij) to the
east < 15' The eastern shore of Wakt'mika is composed of the same
arkose dipping east <12'. These (juartzite-grits on the east side of
Wakemika Lake, as well as those forming the shores of the western
portion of Nonwakaming Lake, occupy the upper part of a low
synclinal basin, resting conformably upon the slates and slaty
greywackes exposed on the southern shores of Wakemika Lake and on
the eastern side of Nonwakaming Lak(^

On the west side of the northern bay of Nonwakaning Lake, the

1 iiish

greenish arkose is overlain by a grayish vitreous quartzite, very V _,,, •
much sheared and broken, the pressure- and fracture-planes being (luartzitc.
coated with brightly glistening scales of yellowish-green sericite. The
rock is made up almost wholly of grayish translucent (juartz with a
lesser jiroportion of felspar, some of which has been converted into this
hydrous form of muscovite by dynanuc action.

The portage from Nonwakaming to Lady Evelyn Lake is about I-"ly ]'.v>'l.vi>
twelve chains in length, and is used to avoid a chute and rapids
below with a total fall of about twenty-tive feet. Lady Evelyn Lake
(so named in 1888 })y Dr. Bell) is known to the Indians as Muskan-
aning (the haunt of the moose). It measures nearly twenty-two miles
in length from the portage entering the south enil to the rocky
obstructed chute which marks the outlet into the ^lontreal River,
The trail reaching the south end shows exposures of greenish slate, Ko^-kf, Hpen.
containing coarser interlaminated beds of a tine-grained greenish-gray
felspathic sandstone, all having a distinctly bedded character. These
partings of greywacke, which vary from a few inches to a foot or even

•ill

.i • i I

266 I

XIPISSIN'C; AM) TKMISCAMING KKCIOX.

Pflf'

!Miei'(i:
cliurat

I'lii.stir

-copical
til' (if
rucks.

Kocks

of wMi
of lak.-

li;irt

more in thickness, veatlior to a pale-purplish colour. The strike
changes from N. 41 " to N. 20' E., the various expt)surcs showing
marked evidences o^ ^L.nsiderable tilting and dislocation ; the angle of
inclination being unusually high, from 38° to 53° in a north- we.sterly
direction. For three miles north of this portage the lake is narrow,
being for the most part either obstructed by tlie loose nuvsses of the
prevailing slate or cut up into a number of channels by a series of
small islands.

The general trend of th'i shores, on either side, corresponds rathei'
closely with the strike of the inclosing slates which is N. 20 E., while
the dip is in a direction of N. 70 W. < 5 to 10 . The hand speci-
men collected as typical of the rock occupying this interval, is a light
gi-eenish-gray fine-grained felsite, of which the jointage-planes are coated
with hydrated peroxide of iron, while the weathered surface exhibited
a pale flesh-red tint. A thin section shows the rock to be; composed
of orthoclase, tjuartz and plagioclase, the iirst named mincTal being
the most abundant, while only occasional individuals of phigioelase
wei-e noticed. The fragments are ^" 'ry uniform in size and show little
or no interstitial matt( r. They are angular or subangular in outline,
frequently interlocking with one another. The section evidently repre-
sents a clastic which has ffull'ered little from atjueous abrasion, while
subsequent incipient reerystallization has concealed, in man}- instances,
some of the rounded outlines due to the action of water. Irregular
scales and plates of chlorite are present, as also a small quantity of iron
ore, the a])undance of the former giving to the whole rock-mass its
decided greenish colour.

About three-quarters of a mile to the south of the large opening
tiiat constitutes the main body of the lake, these fine-grained felspathic
sandstones or felsites are interrupted by a m.tss of medium-textured
diabase that crosses the lake. Northward it extends ahmg tli • east
shore for a distance of over four miles, being succeeded in this dii'ection
by a coujpact finegrained greenish gi'eywaeke that dips to the
west <:10 . On some of the islands lying near this shore, a beautifullj'
banded or foliated tufaceous rock was noticed which is intimately
associated with the diabase. The latter likewise occupies the south-
west shore of the main body of the lake, and also the three large
islands in that neighbourhood as well as a small strip on the western
side, the continuity of the mass being broken by the appearance at the
coast of an area of very massive vitrious pinkish or grayish quartzite
which dips to the west <15'.

For the next succeeding six miles, the lake has an average width of
over two miles, while it is sometimes as much as three miles. A chain

■J

SUAKP KOCK INLET TO MATTAWAPIKA.

207 1

of islands, however, that runs up the centre, as well as a considerable k^.j^^ ,,f tin-
number of islands, both large and small, near the eastern side, conceal i-'lii-iiil^'
niuch of its true size. The islands in general are low and have a souk;-
what irregular outline. Those in the southern part are conniosed of a
dark greenish-gray felspatliic sandstone, witli a decided slaty cleavage,
in places corresponding to certain distinctly alternating bands of
gravish-green colour, which show a prevailing dip to the east < 5 to 12 .
Under the microscope, the rock is seen to be a felspathic sandstone i.itiioin^'ica
maiie up of orthoclase, quartz and plagioclase, imbedded in an abund- L-lianutir.
ant felspathic matri.x, much of which has been decomposed toyellowish-
frieen sericite. This slaty graywacke evidently occurs in a series of low
undulating troughs, for on the west shore in the vicinity of perpendicu-
lar rocky clifls, a somewhat similar rock is seen dipping N. 70" VV. <] 2 ';
while still further north along the same shore the dip is 8. 70" E. --3'.
A hand specimen of the rock fi'om these clifTs, shows a dark greenish-
grav rather fine-grained, felspatliic sandstone w-eathering to a deep
brown colour. Under the microscope it is seen to be composed of
angular, subangular or rounded grains of quartz, orthoclase and
plagioclase, imbedded in a groundmass relatively small in quantity,
composed of a confus:ed aggregate of minute yellowish-green sericite
scales. Occasional fragments of zircon are present and a considerable
quantity of iron ore, some of which is ilmenite, as it is seen
altering to ieueoxene. A large amount of chlorite is present in irregu-
lar scales and plates scattered through the ,'ock, and this, together with
the sericite and iron ore, give the rock ius prevailing dark greenish-gray
colour.

The islands in the northern part of the main body of the lake arc islmuls in

composed of more massive and ciuartzose sandstones, which, as the""'! r'l',
' 1 ' ' jiart ot lake.

Obisaga Narrows is approached, assumes more closely the appearance
and composition of the prevailing arkose.

On the north-east side of the hill, near AVendabin's house, to the l''lesli-r«l
north-west of Lady Evelyn Lake, the arkose shows massive beds of a '
pale llesh-red colour. To the eye the rock closely resembles a granite,
but under the nncroscope its clastic character is clearly seen,
and the texture varying considerably in diffeient parts of the .sec-
tion. Quartz, orthoclase and plagioclase are thickly crowded together
and are connected by comparatively little sericitic matrix. This can,
however, be seen forming at the expense of the felspar. There has
been some enlargement of the grains by subsequent growth, so that in
spite of their clastic character they often interlock with irregular
sutures.*

■*;! ill

* Anmial Ut'iHirt, Ueol. Surv. Can., vol. V. (X.S.), (i. (!8 i'. .Scctiim, No.

1 «s

268 I

NIPISSIN'O AM) TEMISCAMING HKGION.

Country To fhe woHt of Lady Eselyn Lake, the country is comparatively (lat

h'.tcivii Lakf ^''^'' "• t-'onsidcnible (listanco, and is composed, for the most part, of ;i Ihic-

yraincd, somewhat massive dark, greenish-gray greywacke. Thi.s

merges gradually upward into tlie coarse quartzite-grit or arkosc,

(,)ua.tzit,L-grit that constitute tlie range of liigh liills of which Maple Mountain (so-

(It .Malilo ,, . . . . ,.

'1'.
Momitiiiii.

Ohisa^ra
Narrows

called l)y Dr. Bell in 1S8S), the highest part, is situated almost directly
over the western border of the Lake Temiscaming Sheet. Specimens
of the rock obtained by Dr. Bell, in his ascent of the mountain tvmn
the east side, showed the lower portion of this arkose to be a rock noi
unlike a rather fine-grained granite. This is interlaminated with smiiU
greenish bands in which sericite is relatively much more abundantly
developed. The rock was examined by Dr. (i. H. Williams and sliowa
to be an arkose sandstone, although the grains are mostly angular and
often much fractured. They consist of (juartz, orthoclase and plagio-
clase. Neither mica nor chlorite occur in this section, except as a
component of the sericitic grounduia.ss, which is somewhat abundant.
Stains of ferric hydroxide are plentiful and impart the reddish colour
to the rock. At the High Pond on Maple ^Mountain, the rock is a
pale yellowish-gray quartzite, showing distinct, more or less rounded
pebbles, which in appeai'anco closely resemble their matrix. Sericite
is also abundant, visible to the unaided eye. The microscope shows
this rock to be con)posed of angular, or but slightly rounded grains of
granitic quartz, full of iluid inclusions, which are embedded in a ground-
mass of sericite anil finer quartz fragments. These quartz grains or
fragments differ greatly in size, but are under a millimeter in diameter.
Felspar substance is now rare, although once present, it seeins
under the inlluonce of dynamic action to have passed into sericite
or muscovite. In a matrix of this character medium sized
pebbles are embedded. These differ from the matrix pr'incipally in
having a more silicious groundmass, i.e., they are freer from the seri-
cite. They are, however, coated with a membrance of sericite, as is
apt to be the case with squeezed conglomerates or grits. The rock
shows distinct evidences of the action of pressure, and the development
of its mica is probably due to this agency.*

At the Obisaga Narrows, the pale greenish-yellow or pale flesli-i'cd
arkose forms perpendicular cliffs on the south side, a talus of angular
blocks lying at the foot. It occurs in tliick, massive, much jointed
beds dipping to the south-west <28'. This rock occupies the shore on
both sides of the narrows, ^-xtending beyond for a distance of
about three-quarters of a mile, where it gives place to and is underlain
by the banded slate. There is again a gradual transition downward

■* Annual Report, (ieol. Surv, Can., vol. V. (N.S.), p. G3 K

MK1.0W

SHARP ROCK IXLKT TO MATTAWAPIKA.

269

tlirough a massive uiul compact slaty yrcywackt' into the readily cloav-
able and thinly bedded, distinctly handed slate heneatli. This succes-
sion may he well seen on the south shore of this portion of the lake
about three-([uart(!rs of a mile west of the Obisa^a Narrows. The pre-
vailing topof^raphy of the country to the eastward undergoes a marked
chango in outline and from the narrows, known to the Indians as
01)asliin<fwakoka, to the point where the lake turns abruptly to the
uortlnvard, the shores on either side, especially that to the south, are
low and marshy, with only small hillocks, points and beaches of
yellow sand. The lake is correspondingly shallow, with Init a narrow
cliunnel among water-weeds.

r>efore entering the portion of the lake known to the Indians as Xditli.rn
Ko-ko-ko-wa-bikon, and often referi'ed to at the present time as the i".','ilv"]'.'v'(.iy,,
.Mattawapika, (although this name should rightly be restricted in its IjiiUc
application to the immediate vicinity of the outlet of the lake) the
water is divided into two channels, separated from one another by an
intervening low swampy island. The channels on either side are only
about thirty feet in width and both of them show a considerable
current, which is likewise sensibly felt in some of the shallower and
more obstructions portions to the west. A mass of diabase of dyke-
like a.sjiect crosses the eastern point of the island, forming the rocky
barrier broken through by the waters of the lake. The diabase band,
(which is an extension t(j the northward of the large or main mass of
similar rock), is about a (juarter of a mile in width, and runs parallel to
the lake forming its immediate western shore-line for the greater part
of this last stretch before em[)tying into the ^Montreal River. This
western side is, as a rule, steep and precipitous and the basin occupied stecj) cliffs on.
by the waters of this part of the lake has been excavated, for the most " *''<tL''i .side,
part, along the line of junction between the diabase and the neighbour-
ing slates exposed on the east side These slates are banded and rise into
rather prominent and steep eminence, the beds dipping to the east at
low angles. The contact between the two rocks is well exposed
at a point on the west shore about one mile and a half south of
the outlet. The diabase is distinctly intrusive through the slates, dis-
turbing and altering them, while veins of ijuartz containing dissemin-
ated sulphides till the ii-regular fissures formed during the i ' ption.
At the outlet, the slates present beautiful alternating colour-bands of
greenish and purplish shades running with and indicating the lines of
stratification, the dip being to the south-east < 18°. The outlet shows
a series of small rocky islets composed of these slates between and over
the outcropping ledges of which the water pitches in a fine cascade
about twenty-five feet in height. The presence of this chute with its

■1 >'

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IMAGE EVALUATION
TEST TARGET (MT-3)

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fliotographic

Sciences

Corporation

9S WBT MAIN STMIT

WIBSTi£>, N.Y. 14SS0

(716) •72-4503

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,i!»ifcj«.

270 I

NIPISSING AND TEMI8CAMING REGION.

'i ±n

■ i

■'111

Routes from
Hiiilfylmry to
Bay Lake.

Sliarp Lak<'

Portage to
Loon Lake.

rocky environment suggested the name Mattawapika, by which tliis
locality is known to the Indians.

Lake Temiscaming (Haileybury P.O.) to Bay Lake (on Montrka[,

River).

From HaileyV)ury, situated on the west side of Lake Temiscamintr,
ill the township of Bucke, to Bay Lake, on the Montreal River, tlieiv
are two alternative routes. The shorter and more direct, by Sharp
and Loon lakes to the north-east end of Portage Bay, is, however, that
least used, chiefly on account of the greater length of the portages.
But apart from this, the route offers many advantages over the
other. The portage from Haileybury (Matabisataganing) to Sharp
Lake is by a tolerably good wagon-road, a little over six miles in
length, that crosses a somewhat flat country, with, however, a general
slope towards Lake Temiscaming. The rock beneath is concealed by
what seems to be a good depth of soil, composed chiefly of clay,
although in the vicinity of Sharp Lake there arc occasional outcrops of
the greywackt^ slate. The forest growth in this interval is chieHy
remarkable for large specimens of both cedar and poplar, probably the
finest noticed in the whole district.

Shaip Lake (Agwasabanishing) is comparatively narrow, running
north-anil-south, and a little over two miles in length. The northern
portion presents occasional outcrops of the well banded slate, dipping
in a northerly direction at an angle not far removed from the
horizontal. On the west shore of the lake, in close proximity to the
f Hte exposures at the first narrows south of the portage, and extending
for a distance of a (juarter of a mile, are outcrops of a medium-textured
greenish and greenish-gray diabase, which evidently forms the exten-
sion in this direction of the large mass that runs towards Lake Temis-
caming and the Montreal River. The southern half of Sharp Lake has
low, sloping shores, which are for the most part densely wooded and
show no rock exposures of any kind.

The portage to Loon Lake, starts from the bay on the west side near
the southern end of the lake, and is nearly two miles in length, passing
through a level country underlain by coarse sand and gravel.
Loon Lake itself is only about three-quarters of a mile in length, of a
rudely oval outline, exhibiting low swampy shores, composed for the
most part of coarse sand with no outcrops of rock. The Indians call
this lake Ka-mang-onsiwing. The portage from Loon Lake to Bay
Lake is about two miles and a half in length, and also runs through a
comparatively level stretch of country, apparently underlain by

% -"

&AR10W,

r<AKE TEMAGAMI.

271 I

diiibase. A portage between a quarter and half a mile in length
separates Sharp Lake from ^lud Lake (Ka-wabiiish-keewaga) into
which it drains. This is somewhat larger in size than Sharp Lake,
though very shallow, and has the same general direction. The shores of
Mud Lake are low, and there is not a single rock exposure throughout
the whole extent of the shore-line, which consists of coarse sand and
rounded boulders. The portage from Mud Lake to the Montreal
River is a little short of half a mile, running through a sandy flat
between hills of diabase, which rock ocoasionaly, outcrops close to the
path. To the north and east of Mud Lake there are several small
lakes, most of which drain northeastwards towards Farr Creek.
Bass Lake is a beautifully clear and limpid sheet of water, and is
apparently fed by springs. This lake is almost on the same level with
Mud Lake, into which it empties, and from which it is separated by a
short portage.

The portage to Clear Lake, at the head of the west branch of Farr
Creek, starts from the north end of Mud Lake, about an eighth of a
mile south east of that going to Sharp Lake, and is over three quarters
of a mile in length. It passes through woods composed chiefly of
poplar and soft maple, and over ridges of greenish diabase or gabbro,
the summit rising about two hundred feet above Mud Lake. Clear
Lake, as well as the much larger one to the north-east, into which it
empties, and which on account of its numerous islands and bays, is
called Sasaganaga Lake, are surrounded on all sides by well wooded
ridges composed of diabase and gabbro. Fragments of the V)anded
slate were noticed embedded in the eruptive. Both these lakes and
the stream which forms this outlet, constitute portions of a route to
Lake Temiscaming which is now practically abandoned.

Lake Temagami.

Mud Lakf.

Bass Lake.

Clear Lake
and

i^iisngaiiaga
Luke.

ml iillij

r ! ■

This name is of Chippewa derivation, meaning " deep water." Lake
Other names, Temagaming, Temagamang and Tamagamingue, often '■""^^'""
applied to it, are diflFerent methods of spelling the same word,
while the additional ending " ing " or " ingue " is simply a locative aflix
denoting " at " or " towards the place of."

In shape, the lake presents long and often branching arms reaching
out in various directions from a somewhat stunted body. The main
part of the lake, which occupies an approximately central position with
regard to the different large bays, covers roughly an area of about
twenty-five square miles, although the greater portion of this space is

■i :

■1,1

1 ■:

' \ '■

pi 'i

i :. '.

■ , V.

1 ■

„

(

North-cnst
Arm.

Siiitll Wr<t

Ann.

Nortli Ann.

272

xinssixr. a\i» temiscamino rkcjion.

dotted with islands, some of which are of largo size. The water super-
ficies of tlie various hirtjo aim'; represent an additional seventy five
square miles, making a total of one hundred sfjuare miles. It has a
gonoral north-and-south direction, and its greatest length, from the
southern end of tlie .south-west arm to the northern extremity
of Wliitefish Bay, is twenty-eight miles and a half in a straight
line, although the most direct canon channel between the.se two
points measures thirty miles. In width, from the western shore
of the main body of the lake to the portage running to the Cari-
bou Ld<:e portage, it is sixteen and a half miles in a direct line. The
most important of the many bays that form so large a }>art of this
lake, is the North-east Ann, extending from Point Matagama to the
Caribou Lake portage, a littl(> o\f>r twt'lve mile.s, in a direction about
N. 00 E., and varying in width from half a mile to a nnle. To the
.south of this, ]\luddy Water, Cross and Portage bays indent the east-
ern .shore-line, the tirst-mentioned being about four miles long and
lialf a mile wide. The South Arm lies ahnost directly north-and south,
and is about seven miles in length, from a mile to over two miles in
width. The souilu-rn and south-eastern shores present a series of
smaller bays, the largest of which affords an exit to the chief outlet of
the lak", a steep rapid known as the Temagami Chute, .separating these
M'aters from those of Cross jjake. The South-west Arm is almost
completely cut off from t!;e mail) lake by Narrows Island. The con-
necting cliJMinel to the southeast of this island, is very narrow and
crooked, while that between the island and the western mainland has
a width of a little over an eighth of a mile. l''rom this narrows the
bay extends for about time miles, gradually bending around to the
south, which trend is inaintaincd for a little over six miles further,
when it branches into two smallt-r bays, one running to the south-west
and the other to the .south-east for a di.-;tance of about two miles in
each case. The width is very variable, in some cases the shores being
separated by a distance of over two miles, while in the more contracted
portions they usually approach within a quarter or a half a mile of one
another.

To the north, the largest extension has been called the Noith Arm,
from its general trend. Nearly eight miles north of the Hudson's Bay
Company's po.st, this arm is divided into two subsidiary bays, the ea.stern
one being known as Ferguson Bay, running towards the inlet from
Annima-nipissing Lake, a distance of nearly five miles further ; while
the western extension runs a little west of north for about eight miles,
being again subdivided at the upper end into two parts known as
Whitefish Bay and Sharp Rock Inlet. The latter portion is almost

tAmow.

LAKE TEMAGAMI.

273 I

completely separated from the rest of the lake by Deer and Beaver
islands, leaving narrow and crooked channels at either extremity, in
which more or less current is usually discernible, especially after
violent winds from the south.

Between the North and North-east arms, there are several minor BayH U'tween
indentations, known as Ko-ko-ko, Young Loon and Spawning bays. Xorth vjwt
Of these the first-mentioned is the largest, running in a direction a *"""■
little east of north for a distance of about four miles, and receiving at
its head the waters of a rather large lake bearing the same name.
The North-west Ann (Wuskigama) runs a little west of north, with an
average width of over half a mile, for a distance of a little over four
miles from Naipaga Point, when ic changes abruptly to the west,
which general course is maintained, with slight deviations, for a fur-
ther distance of nearly three miles and a half.

Like other lakes of the Archa-an region, this is characterized by great Vast ihhhImt
irregularity of its shore-line and by the vast number of islands with "
which it is filled. These i^ilands vary in size from mere rocks to some
which are several square miles in area and complex in form. As shown
by the detailed survey of the lake, there are over thirteen hundred of
these islands scattered over the surface, the main body of the lake
especially containing a large number.

The most important factors that have determined the distribution of
land and water, are the strike of the foliation or planes of pressure-
cleavage and the unequal resistance offered during the progress of
erosion by the different varieties of the suri-ounding rocks. The
various bays or arms have been excavated for the most part in the
slaty bands, in a direction corresponding with the strike of the foliation ;
while the shore-lines frequently and for long distances are composed of
the liard and unyielding massive diabases or gabbro. As a rule, the Shores of lake
banks of the lake are higli and rocky, in many places, especially where the and wcky.
diabasic rocks prevail, raising in cliffs from a hundred to two hundred
feet in height. Marshy tracts are few and small, and with the exception
of occasional reefs, the water is comparatively deep to within a very
few feet of the shore. Sandy or shingla beaches are, as a rule, rather
rare and of small extent, although at the northern end of the lake,
forming the northern shore of Sandy Inlet (Kawaminashing) there is a
fine sandy shore.

The deepest of a few soundings made, at a point within about Dgpi^j, „f i^jj^^
thirty chains of the western shore of the main body of the lake, was
167 feet, while another within about half this distance from the &ame
18

I 'lii

^^^^Ba

1; Jj ' '

j™pT^— wr-r

274 I

NIPISSlNtt AND TEMISCAMING REGION.

m !

shore, showed 127 feet. About mid-channel between Bear Island and
the group of islands opposite t« the west, the depth varies from 75 to
85 feet. Several soundiQp;s taken at variqus places alxjut the central
part of the channel of the North-east Arm, clearly showed the existence
of a deep and practically unobstructed navigable channel to within a
short distance of the portage to Caribou Lake. The greatest depth was
found about a mile south-west of Broom Island, 120 feet, while in the
centre of the large open space about three miles and a half from the
Caribou Lake portage the depth is only 95 feet. At the several con-
tracted places along the course of the channel the water is much
shallower, the depth opposite the mouth of the Tetapaga Lake being
only 51 feet, while in the narrow.s, about a mile and a hclf from the
portage, the deptli is only 29 feet. The water of the lake is pure and
clear and of a light sea-green tint, while the fish, chietty trout, white-
fish, bass, pickerel, pike and ling, are noted for their si/e and quality.

ClftHtic rocks Th(^ clastic rocks exposed on the shores of this lake include at the
shoivs of'la ke. ^^^^ ^'^^ usual and widespread breccia-conglomerate. This rock has
already been described, and here presents no unusual features
requiring special mention. Here, as elsewhere throughout the region,
it passes upward through a massive dark-greenish greywacke or
felspathic sandstone, comparatively free from the larger fragments or
pebbles, into a banded slate which is the highest member of the
Huronian noticed in the tract of country immediately bordering this
lake. Along the North-east Arm, the prevailing rock is a liglit
greenish-gray sericite schist containing a great deal of quartz in the
form of small lenticular patches and veins running parallel to the
foliation. Iiiterlaminated with t'.iese hydromica schists are rudely
oval patches or masses of a light greenish-gray silicious dolomite. The
quartzose impurities are arrangetl in narrow vein-like forms which
reticulate in all directions through the mass, so that when subject to
ordinary weathering proces.>?es these stand out in relief, leaving irregular
hollow interruptif)ns composed of the softer and more easily dis-
tinguished material. One of these masses occurs on the smaller point
to the east of the outlet from Hay Lake on the north shore, while
several were noticed along the lower portion of the outlet from Teta-
paga Luke as well as at several points along the shore in this neighbour-
hood. A large mass occurs on some islands a little over half a mile
west of the portages into Caribou Lake. The sericite schist curves
around these ovoid masses of impure dolomite, the latter having been
but little deformed by the pressure which has tilted and altered the
schists.

Siiricite-
Rcl)i><t8 and
duluniiteti.

irm

LAKE TEMAOAMI.

275 I

These hydromica schists or slates have evidently resulted from the Origin <)f
,, .. /.Ill • 1 11 liy<iii'iiiica

shearing and decomposition of the Huronian slates, clue to the close schists.

proximity of the two large masses of granite that occur to the north and

south of this bay. It seems probable that these two masses of granite

are united at a short distance below the present surface, and that the

schists therefore occupy a comparatively shallow and narrow trough of

highly inclined strata which have sagged down somewhat into the

originally plastic mass beneath. This supposition best explains the Orifrin <>f

abundance of the quartz veins and masses of pegmatitic or .secondary *'"'"

origin, fs well as the extreme but uniform alteration of the clastic

material, indicating the former presence of an abundant supply of

super-aaturated and heated silicious waters and vapours connected

with the intrusion of the granite. On Ko-ko-ko Bay, likewise, the

clastic rocks have in many places undergone extensive alteration, and

Fig. «.

-M^vr

PKBHI.es in SKKICITK SCHIST,
KO-KO-KO HAY.

the pebbles and fragments of the pre-
vailing breccia-conglomerate are em-
bedded in a highly squeezed sericitic
or chloritic matrix, which has a How-
like arrangement round the inclusions^
caused by the greater hardness of
these ofiering more effectual resistence to the pressure to which the
softer matrix has yielded.

Throughout the whole of the southern part of the lake, the numer-
ous and wide exposures, almost without exception, show the granitic
and diabasic pebbles and fragments characteristic of the basal breccia-
conglomerate ; but in some places the massive greywacke occurring
above is present, while in occasional localities at the north-west point
of High Rock Island and the north-western part of Cross Bay, the
still higher banded slates rise into hills of more than a hundred feet.

The most distinct and persistent structural feature which obtains in Distinct

'^ stnu'tiiral

the more massive forms of the greywackt5 and breccia-conglomerate, is a feature in

pressure-foliation or cleavage. In most places there is little or no
sign of stratification, especially in the basal beds, the pebbles and frag-
ments being irregularly distributed in a massive and compact matrix,
but the colour bands of the overlying slates are a certain criterion of
sedimentation, and these show plainly that the various clastic
rocks lie in low, broad undulating folds, dipping for the most
part at gentle angles. The development of the foliation seems to have
been determined by the pressure exerted during the intrusion of the
large masses of irruptive material with which the clastic rock? are so
intimately and so frequently associated. The breccia-conglomerate
greywacke and banded slates are very evidently graded forms of
18J

l; I

27C I

NIPISSINC AND TEMIHOAMIXC; KKOION.

llfl

Irruptivo

rocks.

ilji

the same rock, differing only in their relative degrees of coarseness
In origin they plainly represent pyroclastic material, and may be
connected generally with the irruption of ilie n)as8ive plutonic rocks,
although the clastic rocks have very evidently been disturbed anil
altered to a certain extent during the progress of their irruption.
Such structural relationship is not, however, inconsistent with known
facts of contemporaneous volcanic action, the associated volcanic ejecta-
menta being frequently pierced and altered by dykes and masses of
tht parent plutonic.

The irruptive rocks present on the lake comprise diabase, gabbroand
granite. The diabase and gabbro are usually intimately associated in
the same mass, differing only in their structure, which is sometimes
macroscopically apparent, but, as a rule, only under the microscojn'.
In composition they are made up chiefly of plagioclase and augite, the
latter usually showing incipient alteration to green triclnoic horn-
blende, while occasionally, especially in the vicinity of certain small
shrinkage-cavities, the reddish-brown augite is completely decomposed
to hornblende that has assumed the actinolitic habit. Usually biotite
is present, sometimes in considerable quantity and some allotrio-
morphic quartz, tilling in the interspaces between the other constitu-
ents. Ilmenite, showing the characteristic alteration to leucoxene,
pyrite, chalcopyrite and pyrrhotite, may also be noticed. A portion
of the north-east shore of the main body of the lake, presents exposures
of coarse tlesh-red granitite, forming the extension in this direction of
the mass which covers so large an area to the north-east. The rock is
exceedingly coarse and massive, often pophyritic, the phenocrysts being
mostly Carlsbad twins of orthoclase, often from one to two inches in
diameter. The biotite, originally present in small quantity, has Iteen
almost wholly converted to chlorite. The whole mass is intersected by
numerous, often large, dykes of pegmatite and fine-grained felsite.

Lakes in area In the area immediately surrounding Lake Temagami are several
wrroiuiding gmall lakes, some of which are worthy of brief description. The largest
ami. of these, Obabica (Rocky Narrows) Lake is about fifteen miles long, with

an average width of over three-quarters of a mile. The inlet, and
the outlet, are situated within three quarters of a mile from one
another, on the west side, near the northern end of the lake. Two
short portages, nearly half-way down the lake on the east side, afford
an entrance through a small lake into the North-west Arm of Lake
Temagami. A short portage separates this lake also from Wawia-
ganid or Round Lake, which extends beyond the western boundary of
the map, constituting an important link in a canoe-route towards the

■ANLOW

]

LAKE TEMACiAMI.

277 I

Sturgeon Rapids, and thence to Wahnapita' Lake. In tlie northern
portion of Obabica Lake, the rock exposed along its somewhat Hat
shores, is the banded green shite, the light-and dark-greenish bands
intUcative of the bedding dipping K.N.E. < 12° to 15°. Diabase comes
out on the eastern shore to the south of the small bay on the route to
Lake' Temagami, while the breccia-conglomerate in very massive bods,
out-crops all along the eastern shore in the southern part, and the over-
lying evenly banded slates at one point on the western shore, form
nearly vertical cliffs of considerable altitude, with a north-westerly
dip <3^

The immediate shores of Round Lake are low, that on the south Uomul Lake,
side exhibiting a good many low hummocks of slate, with intervening
swampy stretches. The western shore to the north of the outlet are
formed by comparatively high cliffs, the lower portion of which, up to
a height of about fifteen feet above the water, is composed of a green,
well banded slate, dipping at a low angle (about 3) to the west, while
superimposed upon this, probably as a sill is a massiv greenish dial)ase
containing abundantly disseminated pyrite. The northern .shores show
only one exposure of slate, the intervening spaces being low and
swampy.

Gull Lake (Gyasgosenda), to the west of the main body of Lake Hcmtf from
Temagami, forms a part of the most direct canoe-route across country WHiiuai)itii'°
to Wahnapitte Lake. Three different routes may be taken from Tema- Lake
garni to Gull Lake. The most northerly is made up of two portages and
an intervening small lake ; the first portage leaving a small bay on the
west side of Lake Temagami, a short distance south of Naipaga Point
at the entrance of the North-west Arm, while the second portage
debouches on the extreme northern end of Gull Lake. A second route
and the one most frequently used, consists of a single long portage,
which goes up a gully on the west shore of the lake directly opposite
the Hudson's Bay Co.'s Post, while a third leaves the South-west Arm,
al)0ut two miles south-west of the narrows, and passing through two
lakes, comes out on the east side of the southern half of Gull Lake.
The canoe-route thence to the Sturgeon River has seven portages, none
of which are of any great length, while the lakes encountered. Turtle,
Manito-peepage and Waw-ashkashing, are all of them rather large and
important.

On the north-west side of Gull Lake, the rock is the greywacke slate, Rocks on

while the eastern shore, as well as the southern part of the lake, show north-west
. , . /T 1 1 , 1 V m. Hide of Gull

outcrops of the massive greenstone (diabase and gabbro). The contact Lake.

between this irruptive diabase and the associated slates, on the most

Ir. !

278 I

NIPIS8INO AND TEMI8CAMINO REniON.

f ■»•

Direction of
contact If-
twcfn »and-
Htont) and
breccia-con-
gl()niernt<'.

(

Niffht Owl
Lake.

•iiiii

I:. I

Canoe-routi'
from main
l>ody of Lakf>
Temagami to
North-eaHl
Arm.

northfrly of the canoe-routes entering Gull Ijuke, comes in near the
south-west end of the first portage from Lake Temagami, the dark
greenish-gray felspathic slates in conjunction dipping S. 70° W. <G5°.

From this point the line of demarcation curves around to the south-
west, striking the east shore of Gull Lake alxtut three-quarters of a
mile from the north end. Crossing Gull Lake, the islands in this por-
tion of which are composed c* slate, it leaves the bay, running to the
south-west immediately north of the narrows. To the south, the con-
tact between the greenish felapathic sandstone and breccia-conglomerate
leaving the west shore of I^ake Temagami, about three quarters of a mile
south of the narrows at the entrance of the South-west Arm, crosses
the first portage on the most southerly of the three routes to Gull
Lake. Thence, with a south-westerly strike, it cuts across the southern
ends of Gull and Turtle lakes, and running to the east of Manito-
peepagee, and parallel to its genunil trend as far as its southern
extremity, where it turns abruptly t<.» the west, crossing the southern
end of this lake, and the small lake on the route immediately to the
west. The slates and felsp.ithic sandstones in conjunction with this
gn^enstoiie are all hardened and otherwise altered in the immediate
vicinity of the contact, while the pressure-cleavage which is the only
visible structural feature, conforms with the line of outcrop of the
diabase.

Ko-ko-ko, or Night Owl Lake, enters the northern end of a narrow
arm or inlet, which bears the same designation, running in a northerly
direction from the main body of Lake Temagami. The shores exhibit
excellent exposures of the breccia-conglomerate on the east side,
with which rock is associated an overlying compact fclspathic sand-
stone. These are penetrated by a massive intrusive greenstone,
chieHy diabase in composition and structure, which occurs in a large
mass coming out on the north-west side of the lake.

Young Loon and Spawning lakes enter smaller bays oft' the east side
of the main body of Lake Temagami, the latter, together with McLaren,
Cummanda and Hay lakes, forming a canoe-route, which, with short
intervening portages affords a means of communication between this
portion of the lake and the North-east Arm, near Broom Island. With
the exception of Hay Lake all are surrounded by hills of a coarsely
crystalline flesh-red granitite, composed chiefly of flesh-red felspar,
grayiah-white quartz and a sparing quantity of chloritized biotite.
Occasional exposures are rather fine-grained, and contain proportion-
ately a greater amount of the coloured constituents, while, on the
other hand, the coarser-grained material is almost entirely free from

LAKE TEMAOAMI.

279 I

he bisilieates. Atone point nonr the soutli end of Young Loon Lake,
a dyke of ihirk -greenish compact material was seen cutting the granite
and running N. 28" K. The contact between the mass of granititt- and
the sericitic schists exposed to the south on Hay I^ake and the North-
east Arm of Lake Temagami crosses about half way over the portage
between Commanda and Hay lakes.

'IVtapaga Creek which enters the Xorth-east Arm of Lake Tenia Tttapaga
gaini, a little over two miles east of Broom Island, serves to drain
Tt'tapaga and Vermilion lakes, which, tog ther with two small beaver,
ponds and Kanichee-kinikisinik Lake beyond, form a short and direct
canoe-route to Net Lake. From the east end of Ti'-tapaga Lake a port-
age runs to Turtle Lake, wliich empties into a bay on the south-west
side near the lower end of Net Lake, and a short carry over st)me
ledges of saricito-schist, from the south .side of Turcle Lakf, atlords an
entrance to the North-east Aim of Lake Temagami to the north of
Ferguson Mine Point. Tetapaga Creek, wliich runs in a south-westerly
direction, is navigable for canoes for a distance of over a mile from the
lake, and a portage of less than half a mile on the south-east ^ide of
the stream, is all that intervenes before Tetapaga Lake is reached.
The rock exposed along the river is the dark greenish-gray and green-
ish hydromica and chloritic schists, striking from N. 50' E. to N. GO'
E., and dipping to the north east < GO^. The.se schists are interfoliated
with occasional large oval patches or areas of a rusty weathering
silicious dolomite.

On Tetapaga Lake, the ro.-k is, for the most part, a li^ht greenish- R(x;k8on

eray sericite schist, nearly vertical in attitude, and with a strike of N. J,'*'*''i'5'' *"°
o J ^ J ' ^ V )'riiiiliiin

78" E. On Vermilion Lake the rock is very similar in character, but Lakes,
has an average stiike of N. 57° E., dipping to the south-east < 80';
wiiile on the south-east shore, a tjuartzose slate contains beds of red
hicmatitic matter interlaminated with others of finely granular magne-
tite. In places the rock is associated with chlorite, and is greatly decom-
posed, showing large quantities of pyrite and pyrrhotite, the whole
striking N. 70' E. and dipping south-Oiist <75 ". On the portage
running northwards from the beaver-pond that lies to the north-east
of Vermilion Lake, the rock exposed is a light greenish gray sericitic
schist, striking from N. 44' E. to N. 59° E., and dipping south-east
<70".

i ! ■

THilMI

IfT

|i)|

iiii I

I. V

liffi

APPENDIX I.

List of Elfaations.

Tlie following elevations were obtained from a careful compilation
of the profilfs of the Canadian Pacific Railway, the Northern and
North-western Division of the Grand Trunk Railway, the location
survey of the Nipissing and James Bay Railway, together with a list
jjublished in I8G0, by Tltoinas C. Clarke, C.E.. in a report on the sur-
veys of the Ottawa Ship Canal. These were corrected by a comparison
with the recently perfected levels of the Uniterl States Lakes Survey,
as published by Mr. L. Y, Schermerhorn in the American Journal of
Science, April, 1887.

The heights of the various lakes on the Mattawa Rivi arc from a
list compiled by Mr. James White, Ceographer to the t jological Sur.
vey of Canada. *

Elevations marked thus (*) have been deduc<'d from actual levelling,
while tilt cbhers have been determined by means of i.ho aneroid
'if^rometer checked at frequent intervals

All heights are in feet above mean tide water at Quebec.

jMileB from
Muntreal.

31S
324
a^O 1
3;<C. 9
343 9

347
357
3tH)

m;v

373
378
38C
389
397
400

/. El<V(itioti3 on CdtuidUin Parifir liailira/i (Muin Line.)

Mattawa

Calvin

Kail Claire

Knthergleu

Bonfield

Nasbonsing

Thorncliffe

Nipissing Junction

North Bay

|Beaucagf

iMtadowsidf .

Sturgeon Falls

Cache Bay

Verner

iWarren

Height in
Feet.

* See Trans. Roy. Soc. Can., 2nd Series, vol. 1., Sec. VI., pp. 188-189.

281

*5«4

•C96

•.591

*837

•782

•785

•(199

•(J74(>

•(569

•(573

•661

•685

•652

•6«>9

•689

i '

Iji

! I ''.

i j

. i

1 fj

i|:|

'% i

illll'i'

282 I

NIPISSING AND TEMI8CAMING BEQION.

Miles from
Junction.

Height in

Fwt.

11 25
24-30

37-95
38-67

45-77

2, Elcvatiom on the Canadian Pacific Raiheay
(Tciiuscariiinij Branch.)

■Junction with Main Line

Snake Creek Siding

Lunisden Station and Siding

Kippawa Junction

Gordon Creek Station

Lumsden Mills Siding

Bridge over Long Lake

Bridge over " Y " Lake

Kippawii Station and Siding

Kippawa Lake Dam

*571
*.543
•551

•580
•593
•801
•831
•801
•885
•883

Miles from
Toronto.

Height in

Feet.

210 9
219-6
223-3

3. Elevations on Grand Trunk Ruilway
(N.iL-If. ir. Division.)

Crossing with the Nipissing and Nasbonsing Railway

Callander

Nipissing Junction

•743
•070
•074

High

Wate.

M j;:;

4. Elevations on Ottawa River.

Ottawa River Junction with Mattawa River (1859.) . . . .

.. 11 „ (1890.)

II II II (1891.

11 II II (1892.)

II t, „ (1893.)

II foot of La Cave Rapids

II head of La Cave Rapids

II foot of Les Erables Rapids

II head of Les Erables Ra[)id8

II foot of Mountain Rapids

II head of Mountain Rapids

II foot of Seven League Lake

II head of Seven League Lake

II foot of Long Sault Rapids

II head of Long Sault Rapids

II head of Long Sault Rapids (1887)

11 head of Long Sault Rapids (1894)

Lake Temiscaming below Presqu'ile

II above Presqu'il*

II below Opiniika Narrow.s

It above Opiniika Narrows

II below Old Fort Narrows

11 above Old Fort Narrows

Lao des Quinze

feet.

•509.5

•509

•506

•503

•507

•509

•519

•520

•532

•533

•540

•542

*591

•591

•691

•591

•592

Mean
Level.

feet.

845

Low
Water.

feet.
•495-2

"-lil5-5
*505
*50(>-31
*.618 03
•.519-13
•522 23
•522-23
•522-73
.522 73
•677 -03
•572
♦571
•577
•577
•577
•577-8
•577-8;
•578 i

WRIOW-

APPENDIX I.

283 r

30800
310 40
310 ■ 80
31(i 25

316 30
310- 85

317 00
318 -20

318 30

319 00
319 01

321 ti5
321-85

322 20
322-35

323 38
321 53

324 71
32518
325.33

to
332 34
33(i 08
339 36

Lcveh on Mattaxoa River

34:

351

9 361
to >
779J
1-98

509

Mouth of Mattawa River

Foot of Plein Chant Kapid and Chute

Head of Lac Plein Chant

F(X)t of Des Epines Rafiids !

Head of Des Lpines Kapida j

Foot of Rapide de Le Rose

Head of Rapide de La Rose

Foot of Ra|)ide des Rochers i

Head of Rapide des Rochers 1

Foot of Rapides des Aipuillej*

Head of Rapides des Aiguilles i

Foot of Chute de Paresseiix '

Head of Chute de Paresseux \

Foot of Little Paresseux Rapids

Head of Little Paresseux Ra|)ids |

Foot of Lake Pimisi (Eel Lake) 1

Foot of Talon Chute I

Head of Talon Chute |

Rapid below Lake Talon ;

Foot of Lake Talon j •639-3

•495-2
•500-6
•517-5
•517-7
•523-3
•523-5
•529-1
•530 5
•535-3
•535-4
•535 8
•535-8
*5()9-6
•569-6
•577-8
•590 6
•590-6
•633 3
*(i33 3
•639-2

Head of Lake Talon

Foot of Turtle Lake ^ •6(»-9

Trout Lake

Lake Nipissing (East Shore)

•667-8
•647-8

•664 1

•666

•640-5

6'. Ltvds on Slurijcon River.

High
Water.

feet.

Lake Nipissing •647-8

Sturgeon Ri\ er, below Sturgeon Falls. , . . . . i

I. above Sturgeon Falls !

t. below Sandy Falls ]

II above Sandy Falls '

i< below Rapids '

II above Rapids i

n below Smoky Falls . . . i

II above Smoky Falls !*73214

M mouth of Tomiko River , i*736'51

I. mouth of Pike River j*74O-60

II mouth of Snake Creek 1*748

11 mouth of Temagami River 1*752

11 at mouth of Maskinonge River.. . . *795

11 at mouth of Wawashkashing Creek

First Liike (on Maskinonge River) . .

Second Lake

Third Lake (Murray Lake)

Fourth Lake

^laskinonge-wagaming Lake

Mean
Level.

feet.

(>46
67tJ
(WO
696
697
703
704

815
813
814
816
826
836

Low
Water.

feet.
•640-5

•722 14
•723-51
•725
•7;%
•735
•785
811

i l^ii.i-^.i^.^

I ill

'-' i

.ii,,: . i

-284 I

NIPISSING A\D TEMISCAMING REGION.

•

High
Water.

feet.

Mean
Level.

Low

•

Water.

G. Li-vt'ls 071 Sturgeon River— Cont,
Sinall Lake (on ICooka&raniii&r Crepk\

feet.
844

864
882
872
871
859
858

"889"
•WO
903
91!)
930
936
951
957
958
959
!M>4

900

903

904

909

911

914

919

920

935

936

990

941

944

956
1003
1004

956

96()

968

983
1008

986

992

994

981

"795"

f.'et.

Kookaganing Lake , . . .

AIcLaren Hiver (at foot of i)ortage from lake)

Mattagomatthing Lake

.Small lake flowing into Walinapitae

Wahnapitae Lake

7. Lcvch on Temayami River,
jVIouth of Temafiranii River.

*752

*735

Island Lake . .

Red Cedar Lake . ...

Head of Swift Current

Head of 3and-bar Rapid

Head of Burnt Portage Rapid

Head of Rapid

Head of Log-jam Rapid

Head of Twin-Rapids .

Head of Flat Rapid

Lake Cross

Temagami Lake

8. Levels on Marten Creek;
Red Cedar Lake

Marten Creek, abf)ve Rapid

II II Swift Current

II II Rapid

II II Swift Current

II II Rapid

II II Falls

11 II Rapids

Marten Lake

Small Lake (on lot 6, con. v, (rladtnan)

11 (on lot 5, con. iv, (Tladnian)

Wicksteed Lake ( Lake)

Forks of Boices and Mackenzie Lake outlets

Boices' Lake

Lower Red Water Lake

Upijer Red Water Lako

Mackenzie Lake

Simpson Lake

Expectation Lake

Desperation Lake

Salvation Lake

Breadalbane Lake

McDiarmid Lake

Fanny Lake

Bush Lake

9, Levels on Tomiko River,
Mouth of the Tomiko River

•73<J-51

*723'51

Tomiko Lake

APPENDIX I.

285 t

.9. Levels on Tomiko River — Cont.

Lake Chelxjgomog

Cameron Lake ,

Tikien Lake

Lake lots 6 and 7, con, iii, {rladinan. .
Lake lot 7, cons, iii and iv, Gladnian .

Kaotisiniinigouang Lake

l'oi>lar Lake

So\ith Spruce Lake

North Siiruce Lake

High I Mean
Water. 1 Level.

feet.

10, Levels on Ottertail River.

Mouth of Ottertail River, on Lake Temiscaining.

White-boa ver Lake (Wabaunk Lake)

Ruth Lake

Beaver Pond (head of river)

*591-8

feet.

798
803
928
930
932
948
949
978
978

Low
Water.

feet.

841
991
091

*577-8

Height.

High
Water.

Mean
Level.

Low

Water.

11. Levels on Matabitchonan River.
Lake Temiscaniing, at mouth of river •. .

feet.

feet.
*o91-8

feet.

feet.
*577-8

vSunmiit of Matabitchouan Portage

927
1247

Beaver Mountain (King of Beavers)

First Bass Lake

858

858-5

859

864
•938
*042
*0o3

965

975

981

991
1006
1022
1027
1029

071

996
1001
1005
1007
1006
1023
1013
1048
1168
1158
1103
1173

Secf)nd Bass Lake

Third Biws Lake

Fourth Bass Lake

Rabbit Lake

White-bear Lake

Crooked or Snaki^ Island Lake

Net Lake

Tiiieving-bear Lake

Small Lake

Small Pond

Lake

. . .

Marshy stretch on river

Small Pond

Mountain Lake (head of Matabitchouan River). .

Ferguson Lake

Duncan Lake

Petrout Lake

Lily Lake

Peeahalx) Lake

Bogie Lake

Granite Lake

James Lake

Waibikaiginaising or Rib Lake

Cliff Lake

Summit Lake

Beaver Meadow

Friday Lake

Wilson Lake

I'll

■|i

•286 I

NIPISSINQ AND TEMISCAMING REGION.

!■'

iH||i

8
I

ill'

Hiuh
Water.

feet.

Mean

Low

Level, j ^Vate^.

12. Lci'ch on Macdonald Greek,
Mouth of Creek on 4th Bass Lake, Matabitchouan River.

feet.

864
914
924
927
927
9.'«-5
934
936
*938

feet.

Cooijer or Macdonald Lake

Small Lake

Glasford Lake

Small Lake ....

Moxam Lake

Biirwasli Lake

Ross Lake

Rabbit Lake South-East Bay

13. Levels on the Montreal River.

Mouth of Montreal River (Lake Temiscaming)

Farm House (liumber Depot) on Long Portage, 860 feet. .

*591-8

*577 8

Summit of Portage, 880 feet

Montreal River at head of Long Portage (3 miles fr mouth)
n above First Ra )id

736
748
760
770
773
793
823
830
836
8()1
869
871
878
882
883
890
890
903
901
911

964

984
1022
1025
1035
1046
1056
1050
1048

993

977

975

935

918-9

900

II „ Second Rapid

1, „ Third Rapid

II foot of Fountain Fal^s

II head of Foimtain Falls

II II Ragged Chute

It above Fourth Rapid

II II Fifth Rapid

II II Hound Chute

II at jwrtage to Mud Lake

II at foot of Sixth Rapid

II at head of Sixth Rapid

II II Seventh Rapid

II at foot of Eighth Rapid

II at head of Eighth Rapid

II Bay Lake

II at mouth of Temagami Branch

Indian Lake

Round Lake (Mountain Lake)

14. Levels on Route, Temagami to Red Cedar Lake.
Lake Temagami

Olier Ijake

Denedus Lake

Wasacsinagama Lake

Beaver Meadow ,

Green Lake

Brophy Lake

Ingall Lake

Jumping Caribou Lake

Upper Twin Lake

Lower Twin Lake

Mann Lake

Norris Lake

Hanging-stone Lake

Red Cedar Lake

15. Levels of Various Lakes.
Pike Lake (Lao aux Broehets) on Gordon Creek

*794

Long Lake, on Gordon Creek

•820-5

rii-ii' iirtir 'liiiwWilll'*-

APPENDIX 1.

287 I

13. Levels of Various Lakes — Cont.

"T"Lake

Lake Keepawa

Summit of portage between Keepawa and DonghiB

Douglas Lake

Little Obaahing Lake

Forest Lake ....

Birch Lake

Devil Lake

Biistien Lake ■

Thompson or McConnell Lake

David Lake

Obashing Lake

Summit of Road between Obashing Lake and Ottawa

River, 942 feet ^

Small Lake at head of Snake Creek on old Winter Road. . . .

Second Lake on Snake Creek on old Winter Road

Long Lake on White Creek

White Lake at head of White Creek

White Beaver Lake (East of McMartins Point)

First Lake on Indian portage-route to Keepawa

Emerald Lake

Small Lake at head of Opimika Creek

Sharp Lake

Mud Lake

Bay Lake

Lady Evelyn Lake.

Non wakaming Lake

Big Whitefish Lake

Lynx Lake

Cole Lake .

Turner Lake

Annima-nipissing Lake

Breeches Ijakes .

Mannajigaina Lake

Trout Lake

Wakemika Lake

Obabica Lake

Wawiagama Lake

Small Lake south of Nonwakaining Lake

ti between Nonwakaniing and Wakemika Lake.

Bear Lake

Angus Lake ^

Free x^ortage Lake '.

Rankin Lake

Miller Lake

Kettle Lake

Lake Niislionsing

High
Water.

Mean
Level.

feet.

*a56
•880

feet.

057
8.52
832
862
8(i2
834
877
874
8ti9
822

781

847

827

852

872

883

1009

11G7

905

900

890

930

955

1010

1025

1045

1057

1070

1085

1075

857

935

932

917

901

960

997

1051

906

970

977

1015

•770

Low
Water.

feet.

*849-6
•870 70

AM-

l^--

t*^ I

■ i

E.
lo(
an
in;
M,

SOI

rec
th(
cai
Bli
aiv
ext
the
not
tlif
Tei
kuc

in t
first
rec(
refe
Got

APPENDIX II.

Y^V

On some Cambro-Silurian and Silurian fosjils from Lake Temis

CAMING, L\KB NlPISSINO AND MaTTAWA OUTLIERS.

By H. M. AMI.

LAKE TEMISCAMING.

Camhro-Silurian (Ordovician.)

In describing the Niagara formation on Lake Temiscaraing Sir \Vm.
E. Logan remarks : — *There are found lying on the Niagara limestone,
loose angular fragments of dolomite resembling tha*^ of the Birds Eye
and Black River formation of Lacloche and Lake Nipissing, and hold-
ing Strophoinena alternata, species of Machirea like M. magna, and
M. Ai/antica, Orthoceraa ancepa, and 0, proteifornv:. He adds : — "The
source of these fragments has not yet been ascertained."

From the assemblage of forms ider tified by the late E. Billings and
recorded in Sir Wm. Ijogan's remarks above, there is no doubt that
there must be represented somewhere in the vicinity of Lake Temis-
caming, one Cambro-Silurian horizon at least, i.e., the Birds Eye and
Black River formation. It remains still to be ascertained whether
any older members of the Cambi'o-Silurian occur under the somewhat
extensively developed Silurian rocks. The Black River formation of
the district, is known so far, only by loose, but angular and, apparently
not far-travelled pieces of limestone. It can scarcely be conjectured
that these pieces of limestone came from any other district than the
Temiscaming area, as there are no outcrops of rocks of Black River age
known in the region to the north of Lake Temiscaming.

Silurian.

Silurian fossils abound on Lake Temiscaming and are well preserved
in the several outliers. From the " Head of Lake Temiscaming" the
first collections were made by Sir Wm. E. Ijogan in 1845. These are
recorded by Mr. E. Billings and enumerated on the page already
referred to. The occurrence of Halysites catennlarla, and of Favosites
Golklandica, was sufficient evidence to enable Mr. Billings to definitely

•(xeokigy of Canada, (18G3,) p. 335.

19 289

"TTTrp

li'i

IS.

290 I

NIPISSING AND TEMISCAMING REGION.

state that the rocks from which thoy came were Silurian. Some
thirteen species were determined at the time.

Notes on certain species.

The collections made by Dr. Bell and Mr. Barlow are very extensive.
One of the most prominent and characteristic features in the fauna
represented, is the prevalence of Corals, not less than seventeen species
of which have been recognized by Mr. Lambe. Of these corals, the
" chain-coral " (Halysites catennlaria) and the " honeycomb coral "
{Favosites Gothlandica) occur in great profusion. They are preserved
for the most part in a silicified condition — nob the best by any means
for study — in a manner much resembling that in which the fossils of
the Black River formation are found at Paquette's Rapids on the
Ottawa River below Pembroke, Ontario.

Few of the higher forms of organisms characteristic of the Silurian
period are found directly associated with the corals, but Clathrodiclyon
vesicidosum, Nicholson and Murie, one of the Hydromedusu*, docs
occur very abundantly and is associated intimately with the corals.

The Crinoidea are very rare ; only three species having oeen recorded
as yet from this basin.

The Annelids are represented by a single specimen of a Conodont,
whilst the Bryozoa, so abundant in certain rocks of the Niagara and
Clinton formations in the province of Ontario and in New York State,
are rather sparsely distributed in the Lake Temiscaming rocks.

Brachiopoda occur in certain bands by themselves and at times
are very abundant. Such is the case with Atrypa reticularis, Linnii'us.
Pentamerus oblongus, Sowerby, a form characteristic of the Wenlock
in England and of the Niagara of the Interior Continental plateau of
Palffiozoic rocks in North America, occurs in vast numbers in a certain
band of yellowish-gray limestone on Mann or Burnt Island.

The Lamellibranchiata or Pelecypoda are very rare, only two genera
having been noticed from all the collections.

The Cephalopoda are well represented, and of these Discosorns
conoideus, Hall, is the most conspicuous and interesting — although the
Orthoceratites include amongst others : — Actinoceraa vertebratum,
Hall, (said to be identical with Actiiioceras Backi, Stokes, described
from the Arctic regions of North America,) and several other forms
peculiar to the Niagara formation of New York and Ontario.

•ARLOW

]

APJ'ENDIX II.

291 I

The trilobites are few. Two forms recorded may be the North
American representatives of the two European species Calymene
Jilumenbachii, Brongniart; and Encrinurua putictatua, Wahlenberg.
The Ostracoda are likewise very rare. A few fragments of Algie occur
in Mr. Barlow's collections and appear to represent two species pre-
viously recorded from rocks of similar age in New York State.

The whole fauna comprises eighty-eight species, representing fifty-
nine genera. These species are for the most part forms referable to
the Niagara formation, although a number of forms, such as the corals
and brachiopods, are also well known to occur in rocks assigned to the
horizon of the Clinton formation.

There are specimens of Favosites Gothlandica from Mr. Barlow's
collection of 189i which measure a little more than fifteen inches in
diameter or over four feet in circumference. The mode of growth of
these Favosites is similar to that described by Prof. G. H. Girty in the
case of Favosites Forbesi var., occidentalis, and very perfect examples
of such large dimensions are not rare on Burnt Island. They exceed
in size and perfection of structure the large masses of Favosites from
the Hamilton formation of Thedford, Ont. Large and small specimens
of this species occur together, and such is the case also with specimens
of the Clathrodietyon vesiculosum, Nicholson and Murie. This is the
species which was described by Billings as Stromatopora concentrica of
Goldfuss. The largest specimen met with measures fourteen, by ten,
by eight inches.

Syringopora verticillata, Goldfuss, was described from specimens
which came from Lake Huron. It is found in tolerable abundance in
the Silurian of Lake Temiscaming. This fact, together with the occur-
rence of several other species which are common to the Silurian of
Lake Huron in the Manitoulin Island, in Michigan and Ontario, assist
in confirming the view that the sea in which the Silurian deposits of
the Lake Temiscaming basin were deposited was connected with the
Silurian sea of the Lake Huron region.

81 :S!:

Notes on Mr, Barlow's collections.

Chiefs Island, Lake Temiscaming. — The fossils from this locality
are poorly preserved, and occur in a rather coarse sandstone showing
clear grains of quartz embedded in a light yellowish-gray dolomite.
The beds from M'hich they were obtained appear to form the basement
or lowermost strata of the Silurian as developed at this point. The
presence of Ualysites catenularia, Linnaeus and of Discosorus conoideus,
19^

■\

292 I

XIPISSINO AND TEMISCAMINK REGION.

|i1^t

"Is

Hall, with other forms from this island serve to indicate the presence
of Silurian rocks on the southern side. These strata which rest uncon-
formably upon the denuded Archtoan rocks, whose surface is very
irregular and uneven, must necessarily have contacts at various horizons
or levels. It would not be at all surprising, indeed, to find arenaceous
beds not only belonging to the Niagara formation and holding fossils
representing different life-zones in this formation, but also similar V)eds
holding older types of organisms, belonging to older formations in the
lower levels of this old Pakeozoic outlier or basin.

Burnt or Mann Island. — The bulk of the large collection obtained
during the years 1893 and 1894 came from this locality. Forty-three
species are represented. The rock in which they are preserved is a
light-yellowish and fine-grained dolomite teeming with the remains of
corals and hydroids. Certain bands, none calcareous, hold brachiopoda
belonging to the species Atrypa reticularis, Linnseus. Several interest-
ing and thin slabs of crinoidal limestone contain crinoid heads as well
as stems. These are of special interest and deserve to be furtlier
studied. It is the only locality on the lake where tolerably perfect
crinoid heads have been obtained, only imperfect fragments of columns
or stems had been noticed previously.

Percy Island. — From this place Mr. Barlow obtained only a few
specimens from which nine species were recognized. Additional
collections from this locality would probably reveal other forms of
special interest. As already stated, the occurrence of Haiysites catenu-
laria and Discosorus conoideus on this island is suflScient evidence upon
which to refer the strata from which they came to the Silurian System.

The Fossil Corals.

In 1896, Mr. L. M. Lambe, of this Department, made a special study
of the corals obtained, and ho has prepared the following lists of
species. —

Burnt or Mann Island, Lake Temiscaming, collected by A. E. Barlon\

1S9S-1S94.

Hcliolitcs ( Plasmopora ) affinis, Billings.
Lptllia Americana, Milne-Edwards and Haime.
Zaphrcntis Stokcsi, Milne-Edwards and Haiine.
Cyathophyllum articulatum, Wahlenberg.
Fdvositcs Oothlandica, Lamarck.
Alveolites Niagarensis, Rominger (not Nicholson).
Limariu (Gnenitei) crassa, Rominger.

■ANiow. J APPENDIX II. 293 I

HaliJtiUt catfnuhtriii, LintiKUH.
ffaliiiitea eom/HH-tu, Kuiuiiiger.
Si/ringoimra hifurcata, Loiisduli-.
S>irinffO]x>ra vvrticiUatu, (iuldfuKs.

North End of Lake Tumiacaminy, collected by R. Belt, 1SS7.

HelMitei suhtithvlatti, McCoy.

2<tphrfnti» Stnkeiti, Miliie-Edwardf) and Hivinie.

Stromboiles piKjmreua, Komiuger.

Fiivositcs Uolhlandiat, Lamarck,

CUidopora crrrirornin, Hull.

Alveolites Niaijurcnsi», Romiiigor (not Nicholnon).

Alvfiilitei aeriatoparoides, Milne-EdwardHaiul Haiine.

Cfvnitcs lunata / Nicholson.

Limaria (Co'nites) crasm, Koininger.

Huliiaites catcnularia, LinnteuM,

Hidi/sitt'S compacta, Roiniiiger.

Siirimjopora Dalmanii, Billings.

Sjiringopora vcrticillata, Goldfuss.

The subjoined table enumerates the SilUrian fossils found at the
several localities in the northern part of Lake Teniiscaming, the
localities and collectors being as follows : —

1. Collection from " Head of Lake Temiscamang " (sic) by Sir W,
E. Logan, 1845.

2. From " North End of Lake Temiscaming," Dr. R. Bell, (sic) 1887

3. Various collections by Mr. A. E. Barlow from Burnt or Mann
Island made in 1893 and 189-t, also part of the " Stewart Collection "
from Burnt Island, obtained in 1892.

4. Percy Island, Lake Temiscaming, A. E. Barlow, 1894.

5. Chiefs Island, Lake Temiscaming, A. E. Barlow, 1894.

! 1!

m 1 ;

i 1 1

294 I

NIPIBSINO AND TEMI8CAMING HKOION.

Table ahotving the genera and i*pecie» of Silurian fosHihJrom
Lake Temiacavdng.

PLANTAE.

Btjthotrcphii grncUis (?), Hall.
II pulmaUt, Hall. . . .

.„ 3 o 8
•B.s W.2S

-. 6 -e 5

HYDROMEDUH.^C.

Clathrodirtiion vcsiculosum, Nicholson and Mnrie.
CfELENTERATA.

ECHINODERMATA.

Crinoidal fragments

Tdxocrinus, n. sp

Dcndrocrinus sp., cf. I). lon^idactyliiH, Hall.
Thi/mnocrinux sp., cf. T. liliiforniis, Hall. ...

ANNELIDA.

Arahdlites,n, sp.

BRYOZOA.

LichcnaJia conccntrica, Hall

Phanopora expanm Hall

Trevuitopora, sp

Cnllopora sp., cf. C. nummiformis, Hall.
Stictopora, sp

Heliolitcs tnhtuhulntu, McCoy *

II (PUtumopom) affinis, Billings |

II sp., cf. J I. Niagarensis, Hall

Ljii'Uia Amerminit, Edwards and Hainio

Zaphrcntis Stoketi, Edwards and Haimu

»!> [

Caninia or Streptelanma, sp i

CyuthophiiUuvi artirulatum, Wahlenln-rg '

II Hj). indt I

Strainhodig pi/jimit'ns, Roniinger

Faronitcn Gothlandica, Lamarck

Chidoftoru ctrvic.ornia. Hall

Alveolites Niaijnrengis, Romingcr

II .icriatoporoiden, Edwards and Hainie

Cnnites luntUa (?), NicholKon

Limarid (Ca-nitea) crauM, Rominger

Haliinten catenularia, Linnieus

II covipncta, Komiiiger

Spriwjopora tifurcuta, Lonsdale I . . . .

II verticillata, (ioldfuss I *

II Daliiutnii, Billings *

1
'£
U

■|

MNLOW

]

AFI'RNDIX II.

Tahlo shounny the genera and sjwciex of Sihirian j'oaails
from Lake Temucaming — Continued.

295 I

BRACHlOl'ODA.

OHhi»(nitlmuMU'i)iir<jantHla,\)»\\i\Ai\

,, Ihtvidmni, df Verneiiil

Lepld-tui trtotsnrndlia, Daliimii

LcplieiM rhomlKiiditUn, Wilekt'iis

Strophonella, »i>

Struphi'vuna, (?) h|)., cf. Lcplo lui corrwjaUi, Conrml.

Choiietia ('/), or .Strophoiiienn (.')

Pldtinstruiihta limx, Kichwivld

Lrpiocii'lM hrmiKphericii, S(»w«rl>y

Atnjpii rctivuUirii, \.' "hbus

II luxioatriittii i i 1

11 iiUirmcdia, lta.ll

lOuinrholrciiui riiiicittK, Daliiian

Hhijiu'lwMlUt mylccta. Hall

II inUriilicata, Hall

II iii-utijilicalii, Hall

II Bp.

Trnnatotipira, up. iiult

Spirifcr, sp., cf. S. Nidimrimiii, Hall

i. Hp. iiidt

Mcrintella didi/mii, Dalinan. .'

II mtvi/ormiii Hall

II sp

Pcntamcnis oblorujus, Sowyrby

^ B

^ .

lei

UASTEROPOlJA.

]iiir(tni<t utiijmom. Hall

Miiirhi.ioni<i KubiiUitti, Hall. . .

II wp. Xo. 1

II sp. No. 2

Loxoncna, n. sp

II 8p

Euomphidus, ii. Hp

Enomphidna alntus, Hisinger .
CiidoaiiiM cunccUatttm, Hall. .
PtdtyostoiiM, Hp

LAMELLIBRANCHIATA.

Mf)diolopsi8, sp., cf. M, crectus, Hall.
Pterincu, sp

CEPHALOPODA.

Diicosorus conoklens. Hall . .
II yracUis ('!), Foord .

M sp. No. 1

II sp. No. 2

• ij'i

■i'i.

■

■ i '

i3 It

lili

i ■

296 I

NIPISSING AND TEMISCAMING REGION.

Table ahotving the genera and species of Silurian fossils
from Lake Temiscaming — Continued.

CEPH.\LOrODA-Co/i^»iHfrf.

Orthoccrat, sp

II Bj)., cf. O. vldvatum. Hall

II »!)., cf., O. viri/iihitti/n, Hall

II SI)., cf., 0. Cadiaus, Billir"" (?- O. subcanctl-

latum. Hall) ,

Orthociran roHilatum, liilliuga

ActinoccntH irrtdiratum. Hail (? A. Backi, Stokes).

TRILOBITA.

Calinncnc Niai/arcnsis, Hall ( — (7. Bbtvienhachii, Brongniait).

niamtti, si> ;

Encrinuru.i, sp., cf. E. punctiitus, Wahlenberg

Proctus, sp

OSTllACODA.

Beynchia, sp., cf. B. hita, Vanuxem.

Isochilina, sp

Lcpcrditiu, sp

References.

1857. Billings, E. — " Report of Progress, Geol. Surv, Canada,
for the year-s 1853-6." Toronto, 1857. On p. 334,
Orthoceras rotulatum is described from the Head of Lake
Temiscaming.

1858. Billings, E. — " Report of E. Billings, palaeontologist,

in Report of Progress, Geol. Surv. Canada, for the year
1857." On pp. 147 and 171 Mr. Billings describes, and
records the discovery of, Syringopora Dahnanii and S.
verticillata, Goldfuss.

1858. Billings, E. — "Canadian Fossils, containing descriptions of
new Genera and Species from the Silurian and Devonian for-
mations of Canada." Extracted from Report of the Geol.
Surv. Canada for 1857. Montreal, 1858, 31 pp.

;i : ft

w^m

lARLOW.

APPENDIX II.

297 I

1863.

1888.

1896.

189(

1899.

Billings, E. — "The Geology of Canada, from the commence-
ment until 1863," pp. 334-336 contains a chapter entitled :
"The Niagara Formation on Lake Temiscaming," m which
two listb of fossils prepared by Billings are given, p. 335.

FooKD, Arthur H. — " Catalogue of the Fossil Cephalopoda
of the British Museum," Part I, Nautiloidea, London,
England, Dec, 1888 : — in which Actinoceras verlebrale is
recorded from Lake Temiscaming.

WiiiTEAVES, J. F. — " Canadian Stromatoporoids," Can. Rec-
Science, vol. V, No. 2, pp. 129-146, Dec, 1897, in which
Clathrodictyon vesiculosum, Nicholson and Murie, is recorded
from Lake Temiscaming.

Ami, H. M. — " Notes on some of the Fossil Orr;«nic Remains
from the Geological Formations and Outliers of the Ottawa
Paheozoic Basin." Trans. Roy. Soc Can., Sec. Series, vol.
II, Sect. IV, 1896-1897, (Ottawa, 1897).

Lambe, L. M. — "Canadian Paheozoic Corals," Ottawa
Naturalist, vol. XIT, No. 11, pp. 219-220, Feb., 1899, where
specimens identified with Cyathophyllum articulatum, Wah-
lenberg, are described from Mr. Barlow's collections on Lake
Temiscaming.

THE MATTAWA OUTLIER.

In the autumn of 1894, Mr. A. E. Barlow submitted for examina-
tion a small but important collection of fossils from a locality on the
north shore of the Ottawa River six miles below Mattawa. The
fauna represented in the pinkish-gray weathering and arenaceous lime-
stones of tb's outcrop is that of the Black River and Trenton. The
presence of Receptacnlites occidentalis, Salter, Orthis tricenaria,Conra,d,
indicate an horizon at the close or summit of the Black River forma-
tion, whilst the occurrence of Prasopora Selwyni, Nicholson, Solenopora
compacta, Billings, ^iajinesqidna alternata, ErL.mons, and Zygospira
recurvirostra, Hall, are eminently characteristic of the Trenton.

The occurrence of this fauna at such a westerly point along the
Ottawa Valley and in such proximity to the Lake Nipissing outliers
on the Manitou Islands, together with the will-known occurrence of
strata of the same age in the islands north of the Grand Manitoulin.
serve to show that in Ordovician times the marine waters of the Lake
Huron Paheozoic basin were directly connected with those of the

i:^r

p'r

298 I

NIPISSING AND TEMISCAMINQ REGION.

■ii

if.!*'

iJII

Nipissing and Mattawa or Upper Ottawa regions. Every species
recorded from this Mattawa outlier has been found in other deposits
in the Ottawa Valley whilst most of them, if not all, are also recorded
from the islands north of Lake Huron.

The following is a list of the species recognized in the collection from
this outlier : —

Protozoa.

RcceptacuUtcs occulentalis, Salter.

EcHlNOnBP.MATA.

Crinoidal fragments, too imperfectly preserved for identification.

They resemble portions of stems of a sjiecies which may be referable
to the genus Olyptocrinus,

Bkyozoa.

Prasopora Selwyni, Nicholson. The microscopic sections prepared of
this form exhibit no variation from typical specimens recorded from
Peterborough, Ottawa, Montreal and other localities in Canada.
This is no donbt the form which received the designations of Favositcs
lycopoditcs, Ouetetca lycopcrdon, and Stcnopora pctropolitana in the
early reports of the New York and Canadian Surveys.

Frondose, and branching Monticuliiroridoe.

Solcnopora compacta, Billings. A form which may probably be refer-
red to this species.

Ccelenterata.

Strrptelasma corniculum, Hall.

Brachiopoda.

Strophomcna incurvata, Shepard.
Eafincsquina altcmata, Emmons.
Orthis, sp., cf. O. tricenaria, Conrad.
(Dinorthis) proavita, Winchell and Schubert.
Zi/ijospira rceurvirosta, Hall.

Gasteropoda.

Loplwspira bicincta. Hall. A young individual referabl to this
species.

Trilobita.

A fragment of a trilobite too imperfectly preserved for identi-
fication.

LAKE NIPISSING— THE MANITOU ISLANDS.

In 1854, Alexander Murray was the first to note the occurrence of
flat-lying limestones on the Manitou Islands of Lake Nipissing. In
his Report for that yeai (p. 124) he refers the occurrence to the

■ARLOW.

]

APPENDIX II.

299 I

Black River formation. " Ormoceras tenuijilum," or as this species is
now called, Actinoceras Bigsbyi, Stokes, is the characteristic form upon
which the determination of the horizon was based.

In 1884, a further collection was made on these islands by Dr. A.
R. C. Selwyn. This was subjected to a preliminary examination by
the writer.

In 1896, a brief note was prepared for the Canadian Record of
Science where seventeen species are enumerated.

In 1889, Mr. T. D. Ledyard, of Toronto, visited these islands
and obtained an interesting collection, which was submitted to Mr.
E. O. Ulrich for examination. The list of species prepared by the
latter and embodied in a paper on the Black River limestone at Lake
Nipissing by Prof. N. H. Winchell, in the American Geologist for
September, 1896, contains besides other forms a number of Bryozoa
not previously recognized from this locality.

In 1892, Rev. J. M. Goodwillie, M.A., of North Bay, made an
excellent collection of the fossils, and communicated them to the
Geological Survey Department at Ottawa. This collection was found
to contain a number of forms hitherto unrecorded in other collections,
and a preliminary study of its contents revealed many interest-
ing species, all eminently characteristic of the Black River formation.

In 1894, Mr. A. E. Barlow collected along the west shore of the
Great Manitou or Newman Island, on the most southerly of the
Manitou islands and on the west shore of McDonald Island. From
the first-mentioned of these collections by Mr. Barlow, a Black River
fauna was detected and Cohimnaria Ilalli, Nicholson, Stromatocerinm
rugosum, Hall, Lophospira helicteres, Salter, and Actinoceras Bigsbyi,
Stokes, recorded, all of which are eminently characteristic. The
presence of Zygospira recurvirostra. Hall, and of a form which is doubt-
fully referred to Phctambonites sericea, Sowerby, from the west shore
of McDonald Island give a slight Trenton facies to the
assemblage from this locality. It may be that further collecting will
reveal a somewhat higher horizon than the zone of Columnaria ffcUli
usually indicates.

The following collections of fossils have been examined by the
writer : —

Manitou Islands, L. Nipissing, A. R. C. Selwyn, 1884.

Manitou Islands, L. Nipissing, Rev. J. M. Goodwillie, M.A., 1892.

West Shore, Great Manitou Islands, L. Nipissing, A. E. Barlow,
1894.

;?M^^I

• 1!

'■'': \

!l !

frir

, r

li!

300 I

NTPISSING AND TKMISCAMING REGION.

\[.

: i

III

West Shore, McDonald Island, L. Nipissing, A. E. Barlow, 1894.

Most souther ly of Manitou Islands, L. Nipissing, A. E. Barlow, 1894.

The subjoined list of genera and species includes all the forms re-
cognized in these as well as in the other collections above mentioned.

Pbotoeoa.

Siroruatoccrium rwjosum, Hull.
Pasccolus i/lohosus, Billings.

C^fiLKNTKnATA.

Colurnnaria Haiti, NicholHon.
Tctradium fihi-atum, SafFord.
Palttophiillum /, ap.
Streptelamna comiculum. Hall.

ECHINODEHMATA.

Crinoidal fragments, too imiierfeetly preserved for idehtification.
Sculptured plate of what appears to be a crystidean referable to the genus
Palccocysites.

BKYOiCOA,

Escharopora svbrecta, Ulrich.

Escharopora limitarts. Ulrich.

Hdopora vmcroimta, Ulrich.

Rhinidictya mutabilis, var. major, Ulrich.

Phyllodictya varia, Ulrich.

BatostoiiM Winchelli, Ulrich.

CaUopora muUitahxdata, Ulrich.

Several other Monticuliporoids raferable to genera and species not yet
examined microscopically, but which apiiearto belong to such geneia
&« Pachydictya, Amplcxopora, Dekayia, Coscinitan, and MonotrypeUu.

BUACHIOPODA.

Strophomena incur vat a, Shepard.

" Trentovcnsis, Winchell and Schuchert

Etijinc. equina alternata, ^Emmons).
Pkctambonitcs icricea, Sowerby.
Orthis tricenaria, Conrad.
Ehynchotrcma incequivalvis, Castelneau.
Zyyospira recurvirostru, Hall.

Gasteuopoda.

Eccyliomphalus Trcntonensis ? Conrad.
Plcurotomaria (Clathrospira) snbconica, Hall
Murckisonia (Lophospira) hclidtrcs, Salter

M 11 hicincta, Hall.

Madurta ' sp. indt.
Fitsispira cloH;/ala, Emmons.
Trochonema nmhilicatum, Hall.

Lamei.lidkanchiata.

Ci/rtodonta Huroncnsis, Billings.
11 CaiMdcmis, Billings.

II sv.hcurinata, Billings.

r:i*i

BARLOW.

APPENDIX II.

301 I

Lamelubranchiata — Continual,

Cyrtodonta sp. indt.
C'tenodonta Icrat't, Hall.
Vanux(7iii(i/ sp. Hall.

Cephalopoda.

Var/inoceras multitulnilatum, Hall.

Oonioceras anceps, Hall.

Actinoceras Biijubi/i, Stokes.

Camcroceras proteiformc. Hall.

Nunno aulcma, Clarke.

Orthoccrus rapax, Billings, or a very closely related species.

II multicatneratuin. Hall.

II anncUuvi, Hall.

M amplicameratum, Hall.

TlULOBITA.

Asaphus, sp. Portion of the hyiMstome of a large individual of this
genus possibly of A. platycephalns or A, sxtsac,

Ostracopa.

Lepcrditia fabulites, Conrad.
Aparchites ncglcctus, Ulrich,

References.

1857.

Murray, Alexander, — " Report of Progress Geol. Surv, Can-
ada, for 1853-6, PP- 101-125, Toronto, 1857. On p. 124
there is reference made to " fossiliferous rocks in the
most western island of the Manitou Group," and Ormo-
ceras tenuifilum, is recorded as evidence of the Black River
age of the rocks in question.

1892.

1896.

Ami, H. M. — "Pala-ontological Notes, No. II. On the
occurrence of Fossil Remains on the Manitou Islands, Lake
Nipissing, Ontario." Can. Rec. Science, vol. V., No. 2
pp. 107-108, Montreal, 1892. Contains a review of Alex.
Murray's paper {loc. cit. supra.) together with a list of fossils
obtained by Dr. Selwyn in 1884, and referred to the Black
River formation.

Ulricii, E. O. — in Prof. U. H. Winchell's paper entitled :
"The Black River Limestone at Lake Nipissing." American
Geologist, vol. XVIII, No. 3, pp. 178-179, Minneapolis,
Sept., 1896. A list of the species of fossils collected by T.
D. Ledyard, Esq., of Toronto in 1889, and determined by
Prof. E. O. Ulrich, is embodied in this paper.

l! - t

i !

■:j*,'

■v!i'»

>:■:?$:

1' i
1

i %

■fl

T f

302 I

NIPISSING AND TEMISCAMING REGIOX.

1898. Whiteaves, J. F. — "On some Fossil Cephalopoda in the
Museum of the Geological Survey of Canada, with descrip-
tions of eight species that appear to be new. Ottawa
Naturalist, vol. XII., No. 6, pp. 116-127, Ottawa, 1898.
Oi> p. 116, Mr. AVhiteaves records the occurrence of Nauno
aulema, Clarke, from the collection made by Alexander
Murray in 1854, from the Black River limestone at Western
Manitou Island (now called McDonald Island), Lake
Nipissing.

lliiffis

•" i

;

.x^-

^ »

ExplanaHon of Colours and signs

Aa.

PR E - CAMS JUAN
Lower Hiuponiaii

Shi/e, con^Umierabe.
Keew^atia

Serix:ite',homblen/ie and cAlorite-scAi^ts;
nuta.sive. ffreenstorieji, CDiabaae, etc);
Jetapiliti I'Iron formation!

IGJSKOCrS
Po St - HiiToni an

80" 16

'^^

tjiiU. Jake

I'A

CANADA

DEPARTMENT OF MINE

GEOLOGICAL SURVEY BRANCH

^ :^

Hon. W. Templeman, Minister; A.P.Low. Deputy Mm
R.W.Brock, Acting Director.

1908

Juint .■ifi^rt X" AM

^'2 ^'*ZiJ7 —

F MINES

BRANCH

ow, Deputy Minister

I I RECTOR.

70'»o

79rifi

7B°

LAKE

'yE.tvn'tiiiion

This diabase is older than thn>v.fll«pt<< sj
ifj.yj*-* Ay which it is surtvifnd^d ■r] '
;>agrf lAq, Part /, Voi.'lXy iHtfj ^k^m

Sheot NV131

Karro wn

a.W.648r

hh'.scHi rri \ f. mhi-s

Pr«-Cambrian

l.owrv Huronintt Shttv utitl t niifflittnf rati

Thr roHfflinnrratf /'ornit tif half <i/' thr Huron-
id n of I Itix district , Thr rovk, tts /I riitr, nirriiM
fruf/tH'-tttMitlrnri»UMrork(if)>t'n. trtiirh rinnjr in
aiif frntn t/if stimtltMt fflrdlrs, to liinil<t<r>' sonf-
ti tm-H Mfrrrttl ffft in it in itftrr. }losi of tit*'

fHliltlis nrt- of vtirioUM tifftr.i of l.imrrntiii n
y mnit'-ti, ttut ijrfvn.itotn' fu'ltltlrs /roni tftf
hrrirtititt tirr oftfn hirntl tt ttltn iiiln nt , mill
itmisionitlln tlii-rf nv ( rtiffinrnt.s of iti.i/tH iff
liffi ml frotn Iht iron /'ornintion of ttir li'tn-ntin,
Tlif fi nr-yvni nfil nintrij- »»/ tlir- '■oni/lnnn-itilr i.%
ii.siHiHif linrkifyf-niHli in rolimt, tinil, iihrrrvvt'
II ni/ ronsiilrmltlf ii-itiini is rxpoHrtI , tin- i on(/loni-
eriiti- fninsrH n p into n .iliitr It if u i/ritil mil ili i-riil.ie
in Hif nnnihi-r, nnti .sin- of thr prhtilt-.i. tir-r liirf/t'
itifUH. hoirrrrr, tlx ii/ifirr hril:. rnnnot In- .t'l nl to
In' trill- tlittfM, ftinrr /irl>l/li;s a ri' of xirrif rinnnion
orrn rrfnri'. Soinr of thr sliili-.s itfr rrrnlif ttiitili'd ,
thr lini'S oj lirilit inif Inimj nnirhril Itfi » roniifiirii-
on.s (tfi nil in f/. Jhr /orinittion , ii.\ n irholi , orriirit
in on ifiiftroj-ininfrlifliorirontiil ftonilion , tmt tlie
utrih*- itnil ilijt fire ronstiititl if vnrffi iiy , itnit
orrnsionilll If thr Inils n n- •ihiir/tfif folilril: hut tnorf
f/rnmillif thr If form a srrirn nj linr hrond itonirs,
rrslinij nnronjorninltlif on thr y ritnitm, or on Ihr
niiturnrd eilffrti of thr Hmriitin irhi.slii. if »a in
Ihr.Hr slatrs and roinfloinrrntrs that nioxt o/ thr
rolialf- liirkri-it rsrnir. silrrr rritiM of Ihr I'ohiill
distrirlorrur. it tiriifhl* rninr on th'- 'itfttrrn
xhoi'r of l.nkr Ti nii.^kii tninff, ifuliim ami rolritr
orrnr, fnrniinp thr inittrij- of a hrrrria nithin
this formation.

iierirnli n

T/iix nfrif'S rtnlirnrrs thr olilrst riirks of' th^
rri/lon, mill ronsint.s liirifrti/ of diirk, or li{fht
yrrrn hornhlrinli-, rhiorilr, ami srvitilr sihintti,
or "ff rrfnstom-.i." JHoit oj' thr rork.H nrr rlmriirl-
rrivi'il hif II in II mil rkril fin riillrl imn of thr
mi nrrnl ronntitiirnlM. tint tin d iffrrmt ra rirtina
.shiiilr into inori- mii.if>iri jornin, or orrnr with
nniillrrrd inassirr liffir.s. It tiinrn, llicgr are
irifh il ifjidillif d isti mfiiinhahlr from thr I'o.st-
II uronian ilinhatir. .IsMorinlrd n'ith thr KrriralCn
f/rrrnstoiirM hordrriny thr northrrn xidr of Ihr
Sorlhrit.Ht Arm of Lakr I imayatni, also in Ihr
nrighhom'hood ot' Austin Itaff at Ihr fool of Ihr
Hoiith arm of thr sanir lukr in thr arm hrlirrrn
Kaytr liork l^akr and F.inrrald l.nkr, arr iridrly
fjrlrndrd oalrrofi.s of thr "iron fornialion"; ivliilr
tnorr local drrrlopmritltt of thr lanit vurkfi orrnr
in thr Vohall rrgion, and in thr dintrirt adjoininy
thr raxl siilr of l.akr Timi/ikmniiiff. Thin ronMi.sIs
hirffely of silirrnnii uiaynrtilr, iiilrrbandrd with
tuirioKHlif rolourndJanprrM and rhrri .with.ln tiomr
tiifftunrrs, a snwil proportion of hrmatitr. With
thr ntorr ttfitiral ffrrrnstonrs. yrrrninh, or yrrif
ish Mint If rnrhs sonirtinirs orrnr, iind a rnnrh

5"'

A (jCfl).

friifdsa

14 V ^ S V * ,

(jcoUtgtAUii bou/uUirie.H

do do undefined

r Glacial strue
/ Strike

/ Dip and strike

/ VerUcai dip
-\~ HorizoTvtal strata
izm' Jleiqhts itv f'eei ahove .sea IcvtU
Poi'. or P. Portaaes
Raji. or R. Jtupvds
Interpi'ovinciaJ Bouiidai;y

(':().Sene<5al,BASc.. /Sew//w/>Aw ami Chief VnuufhUnuUL.
L.N.Rirljard, Jtratuf1u»mm. .

SOURCES OF INFORMS

Sm-vey.'i hv A E. Bartow. l892-ii4, LW5.
Plaits of siwwwi hv ihnvri Land.i Depts
Surveys hv (hnadi/ui Pacific Railway,
(rrolotjty J.J:.BarU>tf.

^ J P 7 s .s- ,

^-~-, H.W.tU7.8

^^ r;

^ Greal AJuiiUou 1.

Sr f—^ (Jfrwmaix I.)

•%L.

, - „ — %jb — ) ?>tmdyqpjILapkli' y-,

' Ctooii<>/Is1iui(Ik

(Tm-

" o

80"

UTinald I.

79°45'

Lou^itude West of Greenwich.

nr-Mf

JoinK S'hrrt ffl!*

SOURCES OF INFORMATION

Hartow. 18^2.94,1^05.

bv (hnvTi Lands Vepts. Ihititrio and Quebec,
aditiii PaeUir Railway.
Barlo*v.

PROVINCES OF ONTARIO AND QUEBEC

Nipisidn^ District Out.imd l^ondur Coimty.{tuo.

(Lake Nijusstug Sheet)

Scale 4- miles to I inch^i

1 o

J&3440
1(>

K 1> 1) Y

U.W.ft4<JB>

L.W. &«»:

Unj) QUEBEC
m-AC CoiuxW. Que.
leet)

At'varn/'uiiyhuf JRcpoH A'.

Second EdiHon

■ L-; i -rfl

15 Miles

I 'I itiniflii ri)ttiur*ii Ifflor* ifil •In fl ,ivtth . • n ■<< ' it
ui.vtitttft-M, u Btnnll ftro/iiirttott .it fiftnotitr. Hith
Iff ninrt- tifftiriil ftr*-r)i>itntfH. iirrrninh, or'trftt-
ish xlntif rtirks %i»nfti mr* oinir. n ini ti tum'h
f t iftnrt'il i/iia rt::ttr in ftmini »»rj t/if .simtht-rit
a/i«<«'<'>>' w/ ilithhif l.iikf, a»nt itl am ritl points un thf
.x/m »•«•««/ /•.'♦if/Zf linrk l.tikf. I'hf vitfifiiM rorkn of
thr hftirtiliH nini' I if at hiijfi unijh'H, tiifi nrr tt/'trn
iliHtiiirtI ff rut iitxt ftnt'i i ntfit btf tnntir.n of
I attir»tinn ffritittirs, Hrtttilvs thf iron orrs

iilrtoilff rrfrrvftt to, thr hfifitlin ri>»»/<f i>i.y, at
tnnfs, frrtnin « Itn rnrtfvistir )n i iifrnls o/ rronomir
itupiirtunrf. A mi tfrnhtrtl hrit fj-ti^nds f'rotn
.Vf/ liikrto tfrtnilion l.oke, thf tno.it ftvotnitn-ttt
tninrral h^inif auri/frous n rm- u o f> 1/ r if e
{ misfnrkfi t. Vht- miffrot is osittilli/ OHHoriatut
with rari/inf/ tfunntitit : i>/ rhnlropiiritf, intritr,
iiinf />i/rrhotit>'. Suttrt- if old htis hffn foiniit on
tCnufilit (itk>- to thf o'f.si of I ,ikv Tititof/atni, in
qnnrlt vina iiKsio'iatvtt irlt/i Hn'tviitiit ntrkt,.

I N K A r

'«"

roui

Poitt- li uroniiin IHttlionf

Lnrqr nrfn» of th*'»'' ♦/«!»•/.•, tmmitirf, tit titnm
i"'rt/ rt'ti rto'-f/i-tii HftI rorkn, o>rit >■ th rinif/hout thf
ffffioii, titnl <trf fftfifiitl It fotiHil riip/tint/ thr
l.oivff H n rttn ill II Mfiiti II ml foiiijlonifvittf. I'hfU
iii'f iiImo foiniil ill fontiirt iritfi most of thf rorJt
tff/tfuoj'thfffffioit, iiHif f/riifrulli/ III >t If iff Kfi-ii to
hiivf thr form 0/ witlflit fxtiintfit , xhfft-likr
tioitim, oftfii ill ilft/irojri iiiiililff li o r 1 z o ii t 11 1
fumitionM. 1 11 mmiifiimtiniri-iithfi/ irrrr firolmlily
fnrmril ni Mitf.i intricitfl into thf ohti-r rorkti, frotn
irhirJi thf oi'frl i/iiiff strittii hnn itiiiri- liffii n tnouftt
tiff frosion. 1 11 thr 1'nloill I'fffioo if i« lifHrvrU
thilt ttir jismirfu notf orrofiivil tiif llif i-olmlt- mlvfr
oris in thi- l.oivfr II 11 roiiiiiii .stiitr unit voiitflom-
frittf, uo-rf firolifilil If /oriiifil lii/ th'- il iitinliiinrf*
irhirh iirrom/miiifil thf i ittrimioii 0/ t/,r ilinlimif.
Hint that th'- orfi mtiif /iiirr tiffii <lfi>o.iilril froin
miiifritt-hfii I'iitff ituitfis 11 n m in- i 11 1 f il ifith thf
i rriiption. In JimifM toirnithifi on thf .Uontrfiil
riffr, nnil t'lilirf toii'iiMhi {> on thf fontfrn nhorfu of
Liilif Timi.ikmninff, t/if ilinfiUMf /.<i rut hif /link
ffliltt/iiith if ffin.s iimuillif rirh in nilritf, anil
i/iiitrts, unit cnrrifiiiff nitrfr-ln'iiiiiif/ minfmls,
1/nlfna, pifritr, n/irrnlitr iron orf. ft,-.

I.niirentiitn li riiniten nntt tfytfi.s/ns

Thf ffritnitf ti/fifx of thf Lnnrentian are ront-
inonlif tiiotitf- tifiiri iiif rarirtifn, iiikI a rr oftm
rnii riif'tfrainfil ii'ith liirfff rriftititla nf ffliinini r.
Thf rofk/i frfifiiriitl It hiirr a fiink, or rf it rotor,
unit tl iMtinrtl ff rut thf iiifiiitifrM of thf KffH'ittin
.ifrifs, lii't a rr innrh olilfr t h 11 n thr l.oiffr
lliiroiiiiiti roniftoiin'riitr, to irhirh thi-if fnriiiitfi
mint ft '»/ t/if fitrloxfil fifhfilffi unit lioiililfru, Thf
ffi-:inilfs on hoth siilrs of l.iikr Ti tiiinkii mi nff
o/i/ifitr to ffrml'- ffniiliiiiflif >iitt> ifiifismr fornm.
rhf lattrr .ihnir iiiiin o ni riiit ion.s, iiiiil oftrn pium
ithriifitlif from 'tioriti -ffiifixs into ffra 11 itf-ffttfiM»,
thf Inttfr tit-inif >>ii fitr rh>- iiKf.it /irmilriit tiffif. In
rertnin amix to th' mst of l.itkf hi/iairn Hif
orriirrrnrf of a riii.H of' rri/stnlli nr liiiifHtonrit, and
Hffihflinf'Mffnitfs of thf tl miriHr Mrrien, ha»
fiffn rffiortrti. Thf Laiimit inn i* nit ti/f nutn
frous fifffinntilf liikfM, irhirh, -n pini'fa, nuiij
j/iflit niiro of frouomic rnluf.

x-iHuiijHiiiyhuf Rrpoii A? 'W,?, fiv Alii'«'tl Ewi«*st Barlow

N" 606

PidcelO <r

Expianal-ion of Colours and signs

Bt 3

^iL J J P. I AN
('lintonaad Nia^ai'a

Limestone. stuiU , rorij^Lomtwat^.

PRE CAMBRIAN
Lower Hioxonian

QiiarUite., aoTU/lom^j'itte
Slate . coruflomerft/e

Keewatin

~] Seficite, hombLende anti. chl/trite^.tchL^ts; \
Att. I ma^.tive- ifreerhStoTiesJDiahaJie.etc.!; |
I Ja^pilit^. (Iiyya formation/

iill'l'lliililii

iGNF.ons
Post Hni'ojiiari

^Dia.

Oiahojie'

Host Keewatiii, iL/nwenUaii)

A (srn),

(infijiti

CANADA

DEPARTMENT OF

GEOLOGICAL SURVEY Bf

Hon W. Tempueman . Mimster; A.PLow, [
R , W. B R o c K , Acting D i p e c

]ao8

CANE

80bo

KENWOOD

KERNS

F MINES

BRANCH

RANCH

w, Deputy Minister,
I p t c r n

Deputy Minister;

.CTOR.

,, „„JIlarP* f\

^l/ i'ouljlOli

■A%

""^IJpSLlnf ^"'- d^.

■'\^^

Sheet N?138

79''oo'

DESfHirm i: \i>rh:s

Pl«;istnccnc

Kjrti'nxi I'f Ufftis wit/tin Iff tonnshi i>s Imri/ti-
iny Ihr hriid u/'l.iikf I'itni.shixmitui H ft- iin-frtd htf
(I fiftiv;/ imi'/ifit of'rliiy, or ■»/ rhti( /»?.».« i'/m/ n)>tfi$.}ils
into sand.

Silurian

I'fn- Sltiifitin ronsi.sln hi i-f/fl y »»/ I itfht- rithni rfil
(imfSto}tfs, iintif rill i ti hif i ntfrxtriit i fi'il niiiijloin-
fViltfM, .111 nil stom.H, iittil .s/i<ilr.s, /'/(« Itrils lif in
m-iirhj /tiirizitntiil nttil inlis, iiml /oi'ni ii /uri/r,
shiilloif, sifitrl i iml hiisiii, i .rtf-nil i ni/ nnrtliirii ril
f')'otn tiif hritil of l.iil>r 'iinii.tl.iitiiintt- I'lirfi iilst>
omiv iit It n iniihi'r nf tiirif uml miiiiiII oiiII i tirs
iffst of tli>' liilii- , null, iiti nil i ntt rrii i>ti-il /riiii/''
itlotif/ I'fA riiMfrrn s/ioi'i ,

Can\l:

an\[)rian

I, Hirer It ii ronian Oini rftitr

The uft/if rnio.it nirmlirr oj't/ir Kiifoninn citnuistt
rhh'jlfi of n iitiii rl : itr, or iirhour, ii.Hiiallfi oj ii /mil:
ffrrrninli,!.rf)rri/ri>li>i,iin<l >s roiii inoiil i) loiir.ti--
f/ril inril. I'/ir roc/> i.< rom/injn il liiri/rlit oj I'riiij-
nirntx of iiMii rt: null Jr/iln/iiir, n ml in filiii'i-.v /iii.K!ir.t
iloirn irn nix into i oni/loni'- rut*-. T/ir lnil.s n ri- ii.siiiil-
lif initSHi ri-, iinil t/i-nf rulti/ lir ivitli roni/m riiti rrl 1/
loir nni/lrs of il i /I. I'/n- /or>nittion, iittinirs, rrnts
irilh n .stronij 11 monforinit 1/ il i ri:rll >i on tlif
Hrririitin or l.ii 11 rrntiii >i , Imt inin/i inorf roin nion -
1 1/ tfif loirrr tnr nili'r /ni.i.sis rii jmll 1/. hut i n.ir ii.'tilil //,
into the .slitir 11 nil rmi'/lonn riiti of tlir n mliil i/i 111/
inrtnhrr 11/ thf l.ium- il 11 rimiiin. I hi' ifim /■tzilf
in till iimi ulioiit 4'olnilt hiis hfvn riill'-il lln I.itr-
riiiiif II rhimr , iiml is rritortnl In rist nnron/nrni-
nhli/ on fill loirrr iiirnihrrs ofthr II 11 ion in n.

I.oirif ft II roniit n Sliitv iinil f onfffonnriit''

Thr roniflonirriiti- j'orni.K t/ir hiisr of Ihr llnron-
iit n of tills it i.<it riit. I'lir r»ch , 11.1 n riili'. rnirii:v
Jriif/nirntn of rii rion.s rwh- tif/ir.s, irhirh riinf/r in
aixr from thr .ininlhsl /n-hhli'.s, to hinililrrs .sonir-
ti niiif .irrrrnl fvft in ilin inrtrr. .Hii.vl of Ihr

/irliliirs lirr of I'lirioii.s tiflir.s of l.iiii rint i n n
{/ritnil's, lull i/rmiifonr in-hhlis from thr
hr'iriiti n itrr oftrn loiitllif tihii nilitnl , unit
orriisionull >/ thi-rf nrr frinjinrnts of jii.t/il ifr
ilrrirril Iroin till- iron f'orninl 'oo o( tin- linn-nti n.
Thr fi n>-<j m i nril tnnlri.r of thr ronf/loiiii fiiti- i.s
ii.siiiillii iliirf 1/ n-rii i sli in rolonr, iitnl, irlirrrrrt'
unit ronyiilr nihil .snlion i.s 1 .ifiosnl , thv romiloni-
rrntr pn.s.sr.s n f> into n sliitr hif n .</ rml mil ilri- rijime
in thi nil nihrr, nnil .si:'' ofthr ftrhhlrfi. Onr liir(/i'
nrrii.s, hoinrrr, thr iififirr lirils rnnniit hr niiiil to
hr f riir slittr.s , .ii nrr firhhxs n rr of rm/ roniinon
orrn rrfnrr. Soin'- of t/ti' -iliitrx iirr rrrnlif hritilml,
thr liiir.s of hrilil i II;/ hriiii/ niilrhril hf/n conx/iir li-
ons hii ml i Hf/. I'lir for Hint ion , 11.1 11 irfioir, orriirH
in II n iiftfiriiji imili t If hori^oiitiil fmiiition , hiit thr
Htrilir II ml ill)) Itrr roii-il'i titl if rii rj/i n;/, unit
orriittiomilh/ Ihr hri/.s n rr .1/111 rjtl 1/ f'olilril : hut more
f/inrriillif thrif form 11 .srrii-s of loir hroitil ilotnra,
rr.itiiiff II nriinfiimiiihl fi on tfir jf rii nitrs, or on thr
iifilii mill flffrs iifthi' Ixrririili n .-irhintn. It is in
thr.ir sliitr.s II ml lonf/lonimttfs Unit m0.1t 0/ thr
rithiilt- ti iri, >l- n r.irn ir- .lilrrr ri'lns of' thr t'ohnlt
it i.itrirf orrn r, .tt H rif/ht'n niinr on thr i,u.it':rn
.ihorr of III hr Vim i.shii i/ii iifi , ifillmit iiiiil riiliitr
in'Ciir, foriniiiy thr mnlri.r nf n hrrrriii irilliin
Ih ii' forinittion.

hrrii'iiti n

This srrirs rniliriirrti thr olilrst rorlts of tlir
rf'iiion, mill ronsints liiri/rlif of iliirli. or Hfflit
firrr.n hornhlrmh-. rliloritr, n ml srriritr nrhi-fts,
or " If rrrn.itonr.i." Most of thr rorl;s iirr rhitrtirt-
rri.ril hi/ 11 inll iiiii rl,ril fni rnllrHsni of thn
mi H'I-iiI ronsliliirnts, Imt thr iliff'rrrnt I'llfirtirit
.sliiiilr into niiirr mitssirr forms, or orrur nith
iinulterril mnssirr ti/firs. .It linifS, thfsr n rr
irith ilif/iriilti/ il istiimnishnhlr from thr I'o.it.
II uroniiin iliiihiisr. .isftoiiiitrii iritli thr Krriritti n
ffrrrnstonrs hovilrri n(f Ihr northrrn siilr of thf
\orthriist .inn of' l.nkr liinaf/inni, nlso in thf'
ni if/hhinirhooit ol .liistin lUi If nl Ihr fool of thr
south II rm of thr sn mr liikr in thr arm hrCwrrn
F.aifir Iforh I ah>- II ml F.inrt'altl fakr, arr iridrlif
rjrlriiilril out r riifL'^ <'/ thr " i ruu fumiat ion" : trhilr
1,11,11 t,-<ii! I. ' "'1 ■>/ fhr .Minir rorhx -III ,11 )'

^t^u^iit^iMim^tikiMtiim

Post Keewatin Lmirf^nt.icm)

A (Jfll). CrTieiUfl

n-z'^-v-rv-:

/"-J

■ ^ «- ^ "

(reolofiiji'aif hou/iJti.ri^'.i

do do und^'M/iied

i' Glacial, strue
/ Strike

so*

/ Dip and .ttrikf

/ Vert.u-<iJ. di/i

T HorCzoTvtiil ."it rata
iZV'i' Urjf^ht^ til t'pfi iibove. Sfi-lfvW
Por Of P Pori/iafS
Rap 1)1- f( RapuLs
[nterpro^anciai Boundary

^'- »%tf^rt>Ai^r'i)M'i^

'I'Too!

80°i8

C-O.Seuecal.RA.Sc, tmtgrvmhrr uuid f'hie-t' Diviufhtanuxii .
L.N.Hicliard mul OEPpudnoinme, J)ra,tuf/it.i>i>en .

SOURCES OF II

Surveys hj A.E.Barlovr. 189.? B4. 190:-.
^^.^Xo\M\^,1^05. Moriey E.Wilson an
Plans ofsurvfiYS by Crown Lands De.^
(re/tloffj b,y A.E. Bariow. O.E.I.ei'oy, J
CohaJt district 6,y W.G.Milli-r ar>,J (
Margiiud, n/)fes hy OAYoiiug

T\rr\\^Kam\n$. W^^Kc

^ \7

80°o6

79'4.b

.Intiis Shrrt ff" l.tl

SOURCtS OF INFORMATION

• IjiY A-E.Barlow. /«y,? H4. 190A 05: O.E.l.eroy, 1903:
iigJ905. Moriey E.Wilsoii €uu1 C.T. i&af>. 1,90S OH 07.
fsurvf^ys 6j' Crown Lands Drpts. Ontario and Qitehec
b,y A.J':.Baiiow.O.?:.T,eroy,G.A.Young and M.E.WUson.
iii«tri4^t by W.G.Milb'r and C yi.Kvi^f^\,(hdario Bureau- of Muwo.
ah n/ttea hy O-AlYbnug

PROVINCES OF ONTARIO asi> (JUKli.
Ni^sstng Imnj'ict Out and Pnntifn- Count]
>'Lake Tuniskainiag Shc^et. ;

Stttursl SoaJe fgStHin

Sca/a 4 milas to I inch

. •'ij

lllll'l'

iiiiiiii!^.

'I'M !' 8«§r^

)iiniy U">'
let.:

IffD QUEBEC

|-i(^ Cofiaty Que.
Sheet:

Second EdiMon

476o

MERCTER

X/PAWA

If f I- It s i> u • ^ h'lf ■ ' I ! ntj : h <^ II t> ' th I r '■ ^ ^ 1 1> '

\ iirth'Ust trill III I'tlif I i iiKHfii mi , i/sn in ('/»<■
iti iijIiliKii rhi'iiil III .liistin liiiji III til'' I'li't <>i till-
siiiilli iiriii iij t/ii'siiiiii liiln' in l/ir n mi liilii-fi-n
l.itiflf Hnil; I iiki' II nil h'.imrtil il lnl;i-, ii ri- niililif
f.rtiHil lit mil I mill iij Ihr "iriiil [niiiinl inn" : irhilr
tiim-r l)i<-iif ilirf/iiiunfiitu 11/ Ihf siiiiif riivlis • itvrii r
ill tlir ( iilnill rfi/iim, tiiiil ill tin ilintrirt iiiljiiin i nt/
tlir fti.sf siilf of l.iiLr I'i ill ixt.ii ni i itff. This I'liimists
liiri/i'/i/ '1/ .\il imiii.H iiKif/mt iti-, i iitevlni nih'il irit/i
rn riiin.sl 1/ rii/oml jiis/n'r.-t it ml rlifrt, ivitli. in .sonii'
inNtiinf'H, It miiiilt fivti/iiift ion nj InHiiititr, tilth
till mill''- tif/iirnl iffifiistiDitn. soiiirl i nifS nriiir,
ff iifiiish. III' i/ffi/ish .tliilif rin'/,s. uinl n niiifh
I I'iirtii rtil i/iiii rt-.itf iit jiiiiiiil iin tlif yoiithi-rn
.sliitii'H nj lUtliliit liikr, II ml lit si'i'vriil fniinl^ tin the
shiivi-Sii] Eiii/lf llnrii l.iilki-. riif rii riiiii.s riirhM iif
till- hi iirnti II iimr lit- iit liiyh <iti)/l'.s, it ml n r*' iifti'H
il i.sti ni'tl ii lilt null fn-nfl riitfil bf) hinliis o/'
I. fin I intiiin ijiitnites. Hfsiiii'.s th-- i tint unit

It/ nitil If rfj'i'iriit ti>, tin lii-i-ii'iil i n i-unfa i ns, nt
films, rirtiiin r/inriirt' lixtir in i nfi-nln iij fvfinijinir
i III liiiftit ifi . I tn i nrrnl iifil lii'll i-.rtfnil,', /'rum
Krt l.iikf to I'frtnilion l.iil,f, tin- initnl /iruini nrni
m I n !• r II I li r i ri i/ ii n »•(/'' roiiK it r s <• n n /< i/ r 1 1 ,■

I itii.ipi<-hr( t. I'lir III i inrill in ii.siiiilt >f ilssnriiitvij
ii'ith fiirifiny i/nitntitifJi n) rhitlvn/nfrifi', fiifrif*',

II nil /iifrrhiititf. Siitiri- i/iilii Iiiih lirrn fniiml nn
Kinivnht liiki- t>> tin- ivi-st of' l,iil;r rimiiijnni i , in
i/mii'ti ri'i IIM ilftain-iiitfil ii-illi Kffifiit i n rnrlix.

Igru'oui
I'ost H iifoniiin IHiiliii>r

Ijiirf/r itmis nj tln-nr ilnih\ nui.i.ii ri-, tit /i)iirx
I'rri/ roil rsf-f/ I'll i lint riirhs, iirriir throiif/hi'iit thr
reijioti, mill n rr I'riifiii nil if loiinil rn /i/ii tii/ thr
IjOll'ir H II I'oti ill II sliltr ilml '•(t/»f//<(>/;»/»»f^. t'ln-lf
II rr illso jiiiinii ill rtintiirt ii'itli most i,f tlir riirii
llffirM III' till' rif/ion. It ml Iff nr mil II inn if hr smi to
hn rr tlir form nj iriiirlif r.rlrinlril , xhfi't-lihr
hoilirx, ojtrn in ii iifiro.ri nintrl if li o r i : n n t ii I
/iiiMitions. In inn n if i nstii nrrs fhrif irrrr /irolnth/if
f'orniril n s sills i nl riiilnl into Ihr oliirr rorli.s. froni
wliirh Ihr iirr rl ifi nif strntii hit.s sinrr lirrn rtinorril
liif minion . In tlir 1'ohiilt n-f/ion it is lirl irrnl
thitt tllf fissn rrs niiir nrrii /liril liif thr roliiill- lilrrr
oris in thr l.oirrr H II run ill n slitl'- unit ninifloin-
rrntr, ivi-rr /n-i>liiililif fi/rimil liif thr it istii lini iirrH
irliirh itrriiin/nt n iril thr intrnsion of thr iliiihiisr,
iiiiil flint th'- orrs niiiif liiirr lirrn ilr)iosili-il ffiin
mi iimil ■ btii rittij irntrrs it s s o r i it t r il iritli tlir
i mi fit ion. In •liimrs tinriiMlii /> on thr Mont mil
rli'rr, II ml I'ltlirr toimshi fi on thr riistrrn shin'rs of
l.itlir I'i ni isli It mi nif , tin- iliiihnsr i.n- rut In/ fihik
f'riils/tiitli ir rriiis iisnn/li/ rir/i in rnlritr iinil
ifiiitft:, itnil III rrifinif sil rrr-brii riiiy m i iirrnis,
ifiilrnii, fii/rili . s/irrnlit r iron orr, rtr.

I II iiri lit in n Ii fit niirs iinri (i nrissrs

t'lir </ rit n it ir tif/irs of' thr Liin rfntii/n it rr roni-
inoiilif liiot itr^ hrii ri nif rnvirtirs. itnil ii rr of'trn
nut rsr- If rn i nril iritli litrf/r rrifsfiils of' frills fni r.

Acetunpartyuuf Rcpoft N'.' Sti^, by Alfr^ecl Eriu^st Biu'low

N°599

Price 10 cts.

Second EdiHon

r.rrfnin itrrn.s to tin- rnst of ,.,,„, ,,,if,,,,,, ,,,r
orrii rrrnrr of ii rrits of r rifstiill i nr I i mrstimrs, nnii
nrfihrl i nr-st/rnifrs of tin H rrnrillr srrirft, hilM
firm rr/toitril. Tin- l.ii iirrnt inn i:i cut hi/ iiiint.
rrinis firifmntilr ifihrs, ifliirli. in )iliirr3, iniiy
isiflil mini lit' »'i'Oti fini i r l-itlllt.

uirlil mini of rrononiir iiifm.

^AQ