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Ontario Geological Survey
Miscellaneous Paper 89
Preliminary Geological Synthesis of the
Savant Lake-Crow Lake
Metavolcanic-Metasedimentary Belt
Northwestern Ontario
and Its Bearing upon Mineral Exploration
by
N.F. Trowell, C.E. Blackburn and G.R. Edwards
1980
Ontario
Ministry of
Natural
Hon- James A- c. Auld
Minister
^ ,^0
Dr. J. K. Reynolds
ReSOUrCeS
Deputy Minister
OMNR-OGS1980
Printed in Canada
Publications of the Ontario Ministry of Natural Resources and price list are
available through the Public Service Centre, Whitney Block, Queen's Park,
Toronto, and the Ontario Government Bookstore, 880 Bay Street, Toronto,
Orders for publications should be accompanied by cheque or money order,
payable to the Treasurer of Ontario.
ISSN 0704-2752
ISBN 0-7743-4876-3
Every possible effort is made to ensure the accuracy of the information con
tained in this report, but the Ministry of Natural Resources does not assume
any liability for errors that may occur. Source references are included in the
report and users may wish to verify critical information.
Parts of this publication may be quoted if credit is given. It is recommended
that reference to this report be made in the following form:
Trowell, N.F., Blackburn, C.E. and Edwards, G.R.
1980: Preliminary Synthesis of the Savant Lake
Crow Lake Metavolcanic-Metasedimentary Belt, Northwestern Ontario, and Its Bearing
upon Mineral Exploration; Ontario Geological Survey, Miscellaneous
Paper 89, 30p. Accompanied by Chart A.
1000-300-80-Sp.
ii
Contents
Abstract........................................................... v
Introduction ....................................................... 1
Geological Setting ................................................ 1
Savant Lake Sub-Area ........................................2
Sturgeon Lake Sub-Area..........'............................ 3
Sioux Lookout Sub-Area ...................................... 3
Wabigoon-Manitou Lakes Sub-Area ......................... 5
Kakagi-Atikwa Lakes Sub-Area .............................. 6
General Stratigraphic Relationships ............................. 7
Preliminary Geochemical Synthesis .............................10
Correlation of Geochemistry with Stratigraphy .................12
Regional ......................................................12
Local .........................................................14
Approach to a Tectonic Model ..................................16
Mineral Deposits .................................................18
Gold ..........................................................18
Savant Lake Sub-Area ................................18
Sturgeon Lake Sub-Area .............................18
Sioux Lookout Sub-Area ..............................18
Wabigoon-Manitou Lakes Sub-Area .................18
Kakagi-Atikwa Lakes Sub-Area ......................19
Base Metals ..................................................19
Volcanogenic Base Metal Sulphides ....................19
Sturgeon Lake Sub-Area .............................19
Savant Lake Sub-Area................................ 20
Sioux Lookout Sub-Area.............................. 21
Wabigoon-Manitou Lakes Sub-Area ................. 21
Kakagi-Atikwa Lakes Sub-Area ...................... 21
Copper and Molybdenum Deposits Associated with Sub
volcanic and Granitoid Plutons ..........................22
Savant Lake Sub-Area ................................22
Sturgeon Lake Sub-Area .............................22
Sioux Lookout Sub-Area ..............................22
Kakagi-Atikwa Lakes and Wabigoon-Manitou Lakes
Sub-Areas ............................................22
Copper and Nickel in Mafic and Ultramafic Intrusions and
Flows .....................................................22
Savant Lake Sub-Area ................................22
Sturgeon Lake Sub-Area ............................. 23
Sioux Lookout Sub-Area.............................. 23
Wabigoon-Manitou Lakes and Kakagi-Atikwa Lakes
Sub-Areas ............................................ 23
Uranium and Other Lithophile Elements..................... 23
Discussion of Mineralization and Exploration Guidelines ......24
Volcanogenic Base Metal Deposits .........................24
Volcanogenic Copper-Gold Deposits .......................24
Gold Deposits ................................................24
Copper-Molybdenum Deposits ............................. 25
Copper-Gold in Intrusive Rocks ............................. 25
Platinum and Platinoid Group Elements ..................... 25
References....................................................... 25
Tables
1 Tentative time correlation of rock-stratigraphic sequences,
Savant Lake-Crow Lake area ................................. 8
2 Base metal sulphide deposits in the Sturgeon Lake .area ..19
3 Base metal sulphide occurrences in the Savant Lake Area 20
Figures
1 Location of the Savant Lake Crow Lake area .............. v
2 Broad lithostratigraphic relationships in the Savant
Lake Crow Lake area ....................................... 9
3 Classification of subalkalic volcanic rocks by Jensen Cation
Plot involving the cation percentages of AI203 ,
FeO + Fe2O3 -i- TiO2 , and Mgd ...............................10
4 Jensen Cation Plot comparing the patterns of variation of komatiitic, tholeiitic, and calc-alkalic rock suites .............. 10
5 Cation plots for Jutten Volcanics, Northern Volcanic Belt, and
Wapageisi Volcanics ........................................11
6 Cation plots for Rowan Lake, Kakagi Lake, Lower Wabigoon
Volcanics, Manitou Section, North and South Sturgeon Lake
Volcanics, Handy Lake Volcanics, and Beckington Road and
Morgan Island Sections of the Northeast Arm Volcanics ...12
7 Cation plots for Brooks Lake, Katimiagamak, Boyer Lake,
Upper Wabigoon and Central Sturgeon Lake Volcanics ...14
8 Composite cation plots for 1191 Samples, Savant Lake-Crow
Lake area .....................................................15
9 Distribution of the three volcanic suites .....................15
10 Chemical variation along a section through tholeiitic to calcalkaline flows and pyroclastics (TCFP) and overlying Fe-tholeiitic flows (FTF) at Wabigoon Lake .......................16
11 Cross-section illustrating hypothetical stage of develop
ment during the time of late tholeiitic to calc-alkaline flow
and pyroclastic volcanism (TCFP) .........................17
Chart
(Back pocket)
A Preliminary stratigraphic units and structural geology, Sa
vant Lake-Crow Lake metavolcanic-metasedimentary belt,
Districts of Kenora, Rainy River, and Thunder Bay.
Ill
Conversion Factors for
Measurements in Ontario Geological Survey
Publications
If the reader wishes to convert imperial units to SI (metric) units or SI units to imperial units
the following multipliers should be used:
CONVERSION FROM SI TO IMPERIAL
CONVERSION FROM IMPERIAL TO SI
SI Unit
Imperial Unit
Multiplied by
1
1
1
1
1
mm
cm
m
m
km
0.039 37
0.393 70
1
1
1
1
cm2
m2
km2
ha
0.1550
3.280 84
0.049 709 7
0.621 371
Gives
inches
inches
feet
chains
miles (statute)
Multiplied by
LENGTH
1 inch
1 inch
1 foot
1 chain
1 mile (statute)
25.4
2.54
0.3048
20.1168
Gives
mm
cm
m
m
1.609344
km
6.4516
0.09290304
2.589988
0.404 685 6
cm2
m2
km2
ha
AREA
10.7639
0.38610
2.471 054
square inches
square feet
square miles
acres
0.061 02
35.3147
1 .308 0
cubic inches
cubic feet
cubic yards
1
1
1
1
square inch
square foot
square mile
acre
VOLUME
1 cm3
1 m3
1 m3
1 cubic inch
1 cubic foot
1 cubic yard
16.387064
cm3
0.02831685
0.764555
m3
m3
0.568261
1.136522
L
L
4.546 090
L
CAPACITY
1 L
1 L
1 L
1.759755
0.879877
0.219969
1 pint
1 quart
1 gallon
pints
quarts
gallons
MASS
ig
19
1kg
1kg
1 1
1kg
1 1
0.03527396
0.03215075
2.204 62
0.001 1023
1.102311
0.00098421
0.984 206 5
ounces (avdp)
ounces (troy)
pounds (avdp)
tons (short)
tons (short)
tons (long)
tons (long)
19/t
0.0291666
ig/t
0.583 333 33
ounce (troy)/
ton (short)
pennyweights/
ton (short)
1
1
1
1
1
1
1
ounce(avdp)
ounce (troy)
pound (avdp)
ton (short)
ton (short)
ton (long)
ton (long)
28.349 523
31.1034768
0.453 592 37
907.18474
0.90718474
1016.0469088
1.0160469088
g
g
kg
kg
t
kg
t
CONCENTRATION
1 ounce (troy)/
ton (short)
1 pennyweight/
ton (short)
34.2857142
g/t
1.7142857
g/t
OTHER USEFUL CONVERSION FACTORS
1 ounce (troyyton (short)
1 pennyweight/ton (short)
20.0
0.05
pennyweights/ton (short)
ounce (troyVton (short)
NOTE Conversion factors which are in bold type are exact. The conversion factors have been taken
from or have been derived from factors given in the Metric Practice Guide for the Canadian
Mining and Metallurgical Industries published by The Mining Association of Canada in coop
eration with the Coal Association of Canada.
IV
Abstract
The Savant Lake-Crow Lake metavolcanic-metasedimentary belt extends for 300 km within the western part of the
Wabigoon Subprovince. Its geologic setting is described
by referring to five sub-areas: Savant Lake, Sturgeon
Lake, Sioux Lookout, Wabigoon-Manitou Lakes, and Kakagi-Atikwa Lakes. Preliminary correlation of stratigraphy
is made between these sub-areas based on the following
observations: 1) general inward facing of metavolcanicmetasedimentary sequences; 2) thick basal mafic as
semblages are all situated at the outer edges of the belt;
3) overlying, mixed mafic to felsic sequences are more in
ternal and contain thick assemblages of mafic flows that
are mostly toward or at the top of these sequences, and
in some places may be allochthonous; 4) association of
clastic sedimentary rocks with mixed mafic to felsic por
tions of volcanic sequences; and 5) lateral continuity of
certain ironstone-bearing formations.
Petrochemical variation diagrams show that the up
ward progression from thick basal mafic sequences to
mixed mafic to felsic sequences is paralleled by a pro
gression from magnesian tholeiitic basalt to mixed tholei
itic to calc-alkalic basalt to rhyolite. Thick mafic assem
blages within or above the mixed sequences are iron-rich
tholeiitic basalt. The mixed sequences are locally cycli
cal. Tectonic evidence is not inconsistent with a model
based on plate-tectonic theory.
Selected individual deposits of gold, base metals,
copper and molybdenum, copper and nickel, and ura
nium are discussed with reference to their lithologic and
stratigraphic setting in the five sub-areas. A discussion of
potential for mineralization, and exploration guidelines,
are given for volcanogenic base metal and copper-gold
deposits, gold deposits, copper-molybdenum deposits,
copper-gold in intrusions, and platinum and platinoid
group elements.
PALEOZOIC
MESOZOIC
PRECAMBRIAN
PROTEROZOIC
Granitic Rocks
Supracrustal
irkland
Lake
0
Figure 1
Scolc of Miles
50
100
Location of Savant Lake-Crow Lake area and its position within the Superior Province.
1SO
Preliminary Geological Synthesis of the
Savant Lake Crow Lake
Metavolcanic-Metasedimentary Belt,
Northwestern Ontario,
and Its Bearing Upon Mineral Exploration
by N.F. Trowell1, C.E. Blackburn1 and G.R. Edwards2
Introduction
Considerable geologic mapping has been carried out by
the Ontario Government in the Early Precambrian metavolcanic-metasedimentary belts of northwestern Ontario
commencing in the latter years of the last century. Until
the 1940s, early work in the Savant Lake Crow Lake belt
(Figure 1), was of a reconnaissance nature (1 inch to 1
mile and greater). Emphasis subsequently shifted to de
tailed mapping (1 inch to V* mile and smaller). Of neces
sity, this tended to be of patchy distribution, located in
areas of known interest to prospectors and exploration. In
more recent years Ontario Government geologists have
embarked on longer-term detailed mapping programs in
specific portions of the belt but these too have tended to
be considered in isolation one from each other.
In recent years geological knowledge has advanced
and concepts have changed at an accelerating rate.
Much of the earlier detailed mapping, excellent and com
prehensive in its time, must now be considered to be in
need of revision and update. This is especially so be
cause it is increasingly being understood that exploration
for economic mineral deposits is facilitated by a sound
knowledge of the depositional and intrusive environments
to which the minerals are related. For example, the ZnCu-Ag-Pb deposits at Sturgeon Lake have been shown
(Franklin 1975, 1976, 1977; Franklin et al. 1973, 1975,
1977; Trowell 1974a,b, 1976, in prep) to be genetically
related to volcanic processes in a distinctive, cyclical, en
vironment.
With these limitations in mind a program was com
menced in 1976 to synthesize and reassess the available
geological mapping throughout the belt. The objectives
were twofold. The primary objective was to determine, as
far as the available information would allow, the geologic
1 Geologist, Precambrian Geology Section, Ontario Geological
Survey, Toronto.
2 Graduate Student, University of Western Ontario, London.
Manuscript approved for publication by the Chief Geologist, On
tario Geological Survey, Aug. 15, 1979. Published with the per
mission of E.G. Pye, Director, Ontario Geological Survey.
history of the Savant Lake-Crow Lake belt. Stratigraphic
correlation and evolutionary trends in petrochemistry and
depositional environments were to be elucidated, with
particular consideration being given to the place of min
eral concentrating processes. The secondary objective
was td assess where future detailed mapping should be
concentrated, so as to aid both future regional geological
re-interpretations and exploration.
The field program involved, over the 1977 and 1978
seasons, a rapid re-assessment of previous mapping
throughout the belt (Trowell et al. 1977, 1978), and the
completion of geochemical sampling of all the major se
quences. The present authors have recently completed
extended studies in the Sturgeon Lake area (Trowell
1970, 1974a,b, 1976, 1977, in prep), the Manitou Lakes
area (Blackburn 1976a, 1979a,c, in prep), and the Kakagi
Lake vicinity (Edwards 1976,1978, in prep) during which
much of the stratigraphic synthesis and geochemical
sampling was initiated.
The present report has evolved from two oral presen
tations, one in March of 1978 when preliminary strati
graphic appraisal and place of mineral deposition was
given at a workshop of the Ontario Geological Survey and
another (Blackburn et al. 1978) giving a preliminary ap
praisal of geochemical information related to stratigra
phy. The present report is intended as an interim report
on this ongoing project. Final results are to be published
as an Ontario Geological Survey Study.
Geological Setting
The 300 km long Savant Lake Crow Lake metavolcanic-metasedimentary belt is situated at the western end of
the Wabigoon Subprovince or Belt (Mackasey et al.
1974). It is continuous with similar lithologies further west
at Lake of the Woods and to the south at Rainy Lake
through to Lac des Milles Lacs. As pointed out by Macka
sey et al. (1974), the metavolcanic-metasedimentary as
semblages of the Wabigoon Subprovince show a pro
nounced northeast alignment, confined to two broad
SAVANT LAKE—CROW LAKE
northeasterly trending lithologic zones now separated by
a large area underlain by granitic rocks. The present area
under discussion is confined to the more northwesterly of
these two lithologic zones (Figure 1).
In a previous comprehensive study, Goodwin (1965,
1970) recognised lithologic continuity along part of the
belt under discussion, and suggested, by implication, its
stratigraphic continuity. For purposes of the present dis
cussion it is convenient to divide the belt into sub-areas
within which there is a good degree of understanding of
stratigraphy and structure. As will become evident, corre
lation between these sub-areas is less well established.
Names of preliminary stratigraphic units and struc
tural features used in the text are shown on Chart A (back
pocket). Stratigraphic terminology is not formalized ac
cording to the requirements of the current code of strati
graphic nomenclature (American Commission on Strati
graphic Nomenclature 1970).
Savant Lake Sub-Area
A series of mafic metavolcanic flows, the Jutten Volcanics
(Rittenhouse 1936) comprise the northwest and southeast margins of the Savant Lake part of the volcano-sedi
mentary belt. On the southeast side of Savant Lake an
approximately northwest-facing homoclinal sequence is
locally interrupted by minor folding. The sequence has an
apparent maximum thickness in excess of 9 km, possibly
up to 11 km. The Jutten Volcanics thin to the south, even
tually disappearing apparently due to intrusion of the Jut
ten Batholith along the plane of unconformity between the
volcanic rocks and overlying conglomerate. The north
west sequence of Jutten Volcanics forms a broad easttrending synclinal structure (Breaks and Bond 1979). The
stratigraphically lowest exposed portion of the Jutten Vol
canics is exposed in the area of Armit Lake (Sutcliffe in
Trowell et al. 1977). Interbedded chert and magnetite,
locally sulphidic, ironstone 1 is situated near the base of
this sequence. In the Neverfreeze Lake area, to the east,
a correlative band of chemical metasediments is found in
direct intrusive contact with granitic rocks (Sutcliffe in
Trowell etal. 1977).
In the Armit Lake area ultramafic sills (Hudec 1965;
Sutcliffe in Trowell et al. 1977) attain thicknesses of 120
m. Locally associated with the ultramafic rocks is a rock
composed primarily of diopside and a zone of recrystallized sediments or pyroclastics.
Trusler (1975) reported that remnants of the Jutten
Volcanics including ultramafic rocks, occur as enclaves
within granitic rocks west of Armit Lake. Remnants of the
1 The term ironstone is used here as defined in the unpublished
classification manual of the Ontario Geological Survey, issued
1978: a chemical sedimentary rock that contains 33 percent or
more of the common iron minerals by volume. This definition ex
cludes other chemically precipitated sediments such as chert,
and clastic sedimentary material, that are commonly interlayered
with ironstone.
Jutten Volcanics can be traced to the west and south as
far as Kimmewin Lake within the Miniss River Fault zone
(Breaks and Bond 1977).
Polymictic clast- to matrix-supported conglomerate
overlies the Jutten Volcanics. The contact is a major ero
sional and angular unconformity (Skinner 1969; Bond
1979; Shegelski and Bell 1976; Shegelski 1978). Ero
sional surfaces and angular discordance between the
Jutten Volcanics and the conglomerate are present.
Granitoid clasts in the conglomerate are locally similar in
lithology to nearby granitoid plutons that intrude the Jut
ten Volcanics (Funk 1973; Kusmirski 1977), indicating
that the Jutten Volcanics were intruded and deformed by
the granitoid plutons prior to deposition of the conglomer
ate.
North and west of Savant Lake, in the Neverfreeze
Lake area and the Kashaweogama Lake area, the con
glomerate, locally grading upward to wacke and siltstone
(Shegelski 1978) passes laterally along strike into inter
mediate pyroclastics, some of which are subaerial, and
mafic flows (Bond 1977, 1979; Shegelski and Bell 1976;
Shegelski 1978). The conglomerate thins to the west
though it can be traced to the north end of Kimmewin
Lake (Breaks and Bond 1977).
Similar conglomerate with finer clastic sediments oc
curs along the south shore of Savant Lake and in the Nev
erfreeze and Elwood Lakes area, though here they were
likely deposited in a more restricted lobe of an originally
continuous sedimentary basin (Sutcliffe in Trowell etal.
1977). Two epizonal porphyry stocks that intrude the met
asediments at Neverfreeze and Elwood Lakes could rep
resent subvolcanic equivalents of pyroclastics interca
lated within the conglomerate.
Volcanism that began with the eruption of pyroclas
tics intercalated within the conglomerate continued with
the formation and deposition of the Handy Lake Volcan
ics (Rittenhouse 1936) comprising a complexly interca
lated sequence of mafic metavolcanics, intermediate and
felsic pyroclastics and redeposited volcanic fragmentals,
subvolcanic intrusions with comagmatic effusive phases,
and wacke-siltstone with thin interbeds of quartz
iron
silicate-magnetite ironstone.
In the Hough-Houghton Lakes area the fragmentals
appear to be of pyroclastic origin whereas to the east and
south they are redeposited fragmentals with intercalated
clastic metasediments (Trowell 1978). In central Savant
Township pillowed and amygdaloidal mafic metavolcan
ics conformably overlie the conglomerate. A serpentinized peridotite, possibly a flow, conformably lies near the
base of these metavolcanics.
The turbiditic wacke-siltstone within the Handy Lake
Volcanics indicates that sedimentation also continued
and that subsequent degradation of the Handy Lake Vol
canics is reflected by the overlying, in part correlative,
wacke-siltstone of the Savant Sediments (Bond 1979;
Shegelski 1978).
The Savant Sediments comprise fine arenaceous to
argillaceous clastic metasediments deposited by turbid
ity currents (Bond 1979; Shegelski 1978) with interbed
ded magnetite ironstone formed as chemical precipitates
of iron and silica originating from a volcanic source (She
gelski 1978).
Sturgeon Lake Sub-Area
At Sturgeon Lake volcanic sequences are folded about
east-, northeast- and northwest-trending axes.
A lower, north-facing, mixed sequence south of Stur
geon Lake, the South Sturgeon Lake Volcanics, has been
shown by recent mapping (Trowell in prep) to be com
posed of four volcanic cycles. Each cycle consists of a
lower unit of mafic metavolcanics and an upper unit of in
termediate to felsic fragmentals. Clastic metasediments
occur locally between cycles. Franklin et al. (1977) con
sider the South Sturgeon Lake Volcanics to comprise only
three volcanic cycles, each cycle comprising a lower unit
of mafic metavolcanics, an overlying unit of intermediate
and felsic fragmentals and an upper unit of metasedi
ments. The massive base-metal sulphide deposits of the
Sturgeon Lake camp are situated within felsic fragmen
tals near the tops of the lower two cycles of Trowell (in
prep) or top of the lowermost cycle of Franklin et al.
(1977).
Laterally extensive mafic metavolcanic flows form
the base of the South Sturgeon Lake Volcanics. Massive
flows predominate but rare, finely amygdaloidal and mi
nor porphyritic flows are also present. Pillowed flows and
autoclastic/pyroclastic fragmentals occur at the top of
this lower sequence. The flow structures and textures in
dicate initial deep water outpourings of mafic lava build
ing up a broad basaltic (shield) volcano.
Upwards, cyclic volcanism dominates. Mafic flows
are massive and pillowed and show an upward increase
in vesicularity. Intermediate to felsic fragmentals, with
rare felsic flows, are predominantly of redeposited pyroc
lastic and rarely autoclastic breccia origin. Upper frag
mental units show evidence of having formed by explo
sive volcanism in a shallow water to subaerial
environment. Shales, graphitic shales, and sulphidic
(graphitic) ironstones are situated within or overlie upper
felsic fragmental units. A major unit of laterally extensive,
north-facing, clastic metasediments tops the South Stur
geon Lake Volcanics.
The character of this mixed sequence is akin to se
quences developed in modern-day island-arc stratovolcanoes.
North of Sturgeon Lake, the predominantly southfacing North Sturgeon Lake Volcanics likewise show a
cyclical development of volcanic stratigraphy. White
comprising the north limb of the Sturgeon Lake syncline,
this volcanic sequence is not strictly correlative, either lithologically or chemically, to the South Sturgeon Lake
Volcanics of the south limb (Trowell in prep.).
To the northeast, the North Sturgeon Lake Volcanics
are correlative with the lower half of the Northeast Arm
Volcanics. Further to the north, distal tuffaceous units of
the Northeast Arm Volcanics interfinger with similar units
of the Handy Lake Volcanics. Upper volcanic units of the
Northeast Arm Volcanics either represent fold repetitions
of lower units or are correlatives of the Central Sturgeon
Lake Volcanics that overlie both the North and South Stur
geon Lake Volcanics.
The Central Sturgeon Lake Volcanics comprise pil
lowed and amygdaloidal flows and autoclastic units. Mi
nor intermediate flows and fragmentals locally comprise
the top of the sequence. Ultramafic and mafic intrusions
are situated between lower flows and upper fragmental
units.
The Sturgeon Narrows Structural Zone transects the
Sturgeon Lake volcano-sedimentary belt. The zone is
probably an early structure, along which later rifting oc
curred, associated with emplacement of the Sturgeon
Narrows and Squaw Lake alkaline complexes that intrude
the volcano-sedimentary belt. Late movement along this
zone is indicated by breccia, shear, and mylonite zones.
Sioux Lookout Sub-Area
The volcano-sedimentary belt between Sioux Lookout
and Wabigoon Lake is composed of five major lithostrati
graphic units. Except for assigning the Patara Sediments
of Pettijohn (1934,1935) to potential group status (Trowell
in Trowell et al. 1978) due to the wide diversity of lithologies found within it, the terminology of Turner and Walker
(1973) is followed for naming these lithostratigraphic
units.
The Northern Volcanic Belt comprises a lower, pre
dominantly south-facing mafic metavolcanic sequence
herein named the Botham Bay Volcanics (not labelled on
Chart A) and an upper mixed intermediate to felsic metavolcanic-metasedimentary sequence, the Patara group.
Flow structures and texures such as vesicularity and
pillow form were initially the parameters used to subdi
vide the Botham Bay Volcanics. Subsequently, wholerock chemical analyses of samples collected during the
present study indicate that these subdivisions are in gen
eral a reflection of their chemistry: either high-magnesian
flows (rounded to amoeboid-shaped pillows, non-amygdaloidal) which predominate, or high-iron flows (bunshaped pillows, large amygdules) respectively. Recum
bent-style folding has repeated portions of the Botham
Bay Volcanics at Vermilion Lake. High-iron tholeiitic meta
volcanic flows have locally been thrust faulted into their
present observed position between high-magnesian
flows.
An interbedded chert and quartz-magnetite (locally
sulphidic) ironstone unit is locally found at the top of the
Botham Bay Volcanics. Clasts of similar lithology to this
unit are found in the unconformably overlying conglomer
ate of the Patara group (Johnston 1972; Trowell in Trowell
efa/. 1978).
The Patara group has three main components: (1)
clastic metasediments of volcanic derivation; (2) interme
diate to felsic pyroclastics, redeposited volcanic frag
mentals, and derived conglomerate; and (3) quartz porphyry/felsite hypabyssal subvolcanic rocks (Johnston
1972; Trowell in Trowell et al. 1978). On the basis of the
distribution and interrelationship of these three lithologies
it appears that volcanism was contemporaneous with the
SAVANT LAKE—CROW LAKE
deposition of the upper clastic metasediments of the Patara group and continued during and following deposition
of the Ament Bay Formation (Turner and Walker 1973) of
the Abram Group (Trowell /ntrowell etal. 1978). With this
proviso of concomitant volcanism and sedimentation the
stratigraphic subdivision of the Abram Group by Turner
and Walker (1973) is still applicable with respect to the
description of lithologies and is followed in this paper.
The Abram Group comprises the Ament Bay, Dare
devil, and Little Vermilion Formations (Turner and Walker
1973; Trowell in Trowell etal. 1978). The Ament Bay For
mation is composed of granitoid-clast conglomerate and
arkose. It exhibits an unconformable to locally conforma
ble relationship to the underlying Patara group. Distribu
tion of lithologies and observed sedimentary structures
indicate a change in the environment of deposition from
subaerial alluvial fan deposition (Turner and Walker 1973)
to possibly braided river deposition (Trowell in Trowell et
al. 1978).
The Daredevil Formation appears to be both interca
lated with and overlying the Ament Bay Formation. It is
composed predominantly of intermediate to felsic tuff
with minor mafic tuff and wacke-siltstone at Little Vermi
lion Lake.
The Little Vermilion Formation overlies the Ament Bay
and Daredevil Formations. It is composed of sedimentclast conglomerate and wacke-siltstone likely deposited
by turbidity currents. Its interpreted environment of depo
sition is in marked contrast to that of the Ament Bay For
mation beinq more akin to that of the Minnitaki Group (see
below).
The Abram Group faces predominantly south with
minor reversals. The Little Vermilion synclinal fold and its
eastern extension are faulted out along the Little Vermi
lion Fault. An outcrop of sediment-clast conglomerate oc
curs along the north shore of the west portion of Abram
Lake. It could be the lateral correlative or the fault-dis
placed equivalent of the similar unit at Little Vermilion
Lake. Silicate-quartz-magnetite ironstone is interbedded
with thickly bedded graded wacke units at the east end of
Abram Lake, and possibly continues northeast along the
length of Botsford Lake (Page 1978b).
The Central Volcanic Belt is composed dominantly of
metavolcanics with minor wacke and siltstone of volcanic
provenance. In the eastern portion of the area a felsic metavolcanic sequence exposed at Superior Junction and
extending to the northeast (Page 1978b) and southwest
(Johnston 1972) apparently lies at the base of the Central
Volcanic Belt. It is composed of felsic pyroclastic and au
toclastic breccia, possible flows, subvolcanic intrusive
material and minor mafic flows.
A broad laterally extensive assemblage of mafic
flows (Page 1978a; Trowell in Trowell etal. 1978) overlies
this basal sequence. Thin interflow beds of intermediate
to felsic tuff and wacke units of volcanic provenance
characterize this assemblage.
An assemblage of mafic to intermediate flows and
fragmentals of basalt and andesite composition overlie
the lower mafic flow sequence. This assemblage may be
unique to the Savant Lake Crow Lake area both in the
vast amounts of andesitic material and in the unique
chemistry of the andesites themselves (Page 1978a).
Quartz-feldspar porphyry/felsite and trondhjemite
plutons of probable subvolcanic origin intrude the Central
Volcanic Belt. They are similar in texture and composition
to intrusions within the Patara group described above
though no time equivalence has been established.
In the eastern portion of the area the Central Volcanic
Belt appears to be fault-bounded against both the Abram
and Minnitaki Groups. To the southwest actual contact re
lationships are not known but faulting, possibly with a
thrust component, is suspected.
The Minnitaki Group is predominantly composed of
wacke-siltstone, arkose, and granitoid-clast conglomer
ate. The granitoid clasts are predominantly quartz-felds
par porphyritic trondhjemite and equigranular trondhjem
ite and were likely derived by erosion of hypabyssal
subvolcanic intrusions and unroofing of-subjacent grani
toid rocks. The conglomerates are mainly confined to the
area of East Bay, Minnitaki Lake and continue only a short
distance to the east (Page 1978b). They have been inter
preted as proximal turbidites of the resedimented associ
ation (Walker and Pettijohn 1971). To the southwest finer
grained wacke-siltstones are of the deep water turbidite
association.
Whether the Minnitaki Group is the folded equivalent
of the Abram Group as Johnston (1972) suggested or
whether it is a younger clastic metasedimentary se
quence as suggested by Turner and Walker (1973) has
not been resolved.
The metavolcanic sequences in Pickerel Township
could be intercalated within rather than infolded (John
ston 1969) with the Minnitaki Group metasediments.
To the southwest in the vicinity of Dryden, metasedi
ments laterally equivalent to the Minnitaki Group are
bounded to the south by the Wabigoon Fault. Similarly in
the area of Southeast Bay, Minnitaki Lake the Minnitaki
Group is in fault contact with the Southern Volcanic Belt.
There are places however where the boundary of the Min
nitaki Group and Southern Volcanic Belt are irregular and
not obviously fault controlled (P. Palonen, Geologist, On
tario Ministry of Natural Resources, personal communica
tion 1978). Splay faults with a thrust or strike component
off the main fault could account for these local irregulari
ties.
The Southern Volcanic Belt lies along strike from,
and appears to be correlative in part with, the Central
Sturgeon Lake Volcanics, the youngest volcanic assem
blage in the Sturgeon Lake area. Here andesite and ba
salt flows and fragmentals overlie the mafic flows in the
area between Flying Loon Lake and Whiterock Lake. It is
possible that these andesites and basalts are correlative
with the sequence of similar composition within the Cen
tral Volcanic Belt. If so, the Southern Volcanic Belt may
be, in part, correlative to the mafic flow sequence under
lying the andesites of the Central Volcanic Belt. Interme
diate volcanic flows are also present in the general Southeast Bay, Minnitaki Lake area (Bartlett in Trowell et al.
1978).
A zone of dominantly intermediate to felsic pyroclas-
tics occupies the northeast region of Southeast Bay, Minnitaki Lake (Bartlett in Trowell era/. 1978) and extends an
unknown distance to the east. It is composed of lithic tuff,
heterolithic tuff-breccia and minor crystal tuff.
Ultramafic and mafic intrusions occur in the lower
portion of the Southern Volcanic Belt (Bartlett in Trowell et
al. 1978; Palonen and Speed 1977; P. Palonen, personal
communication 1978).
In the southwest part of the area the Southern Vol
canic Belt is predominantly northwest facing. Folding oc
curring in the vicinity of Southeast Bay, Minnitaki Lake
(Bartlett in Trowell et al. 1978) was also noted by Pettijohn
(1937) in the eastern extention of the lake.
Wabigoon-Manitou Lakes Sub-Area
At Eagle and Wabigoon Lakes, volcanic sequences are
essentially north facing, as was recognized by Moor
house (1941) and Satterly (1943). However, at Eagle
Lake, the lower part of these Wabigoon Volcanics (Sat
terly 1943) are folded about three northeast-trending
axes, and the top of the sequence is folded about a num
ber of tight east-trending folds close to its northern
faulted contact (Blackburn in Trowell et al. 1977, Black
burn 1979b).
At Wabigoon Lake the lower part of the sequence is
composed of pillowed mafic flows intercalated within a
heterogeneous assemblage of tuff and lapilli-tuff pyroc
lastics and volcanic-clast metasediments. At Eagle Lake
the stratigraphically equivalent lower part of the se
quence is predominantly composed of pillowed mafic
flows. Mafic and ultramafic intrusions occur at the base of
the lower sequence at Mile Lake and at Nabish Creek.
Felsic pyroclastics and flows appear to be concentrated
toward the top of the lower sequence, notably near cen
tral Eagle Lake and central Wabigoon Lake. Recent field
investigations (this study) show that subvolcanic felsic
phases near Meridian Bay of Eagle Lake pass gradationally into granitic phases of the Atikwa Batholith with which
they are therefore genetically related. Similar relation
ships may be present between rhyolites just east of Con
tact Bay and rocks of the batholith at Contact Bay of Wa
bigoon Lake.
At both Eagle and Wabigoon Lakes the lower se
quence is overlain apparently without a break by a pre
dominantly pillowed mafic flow sequence, characteristi
cally amygdaloidal and with large pillows (Satterly 1941,
1943). Mafic and ultramafic intrusions occur within this
upper sequence at the town of Wabigoon.
For descriptive purposes, the upper and lower se
quences of the Wabigoon Volcanics are respectively
named the Upper Wabigoon Volcanics and the Lower
Wabigoon Volcanics in this paper.
Further south, in the Manitou-Stormy Lakes portion of
the belt, correlation of volcanic units has been made
(Blackburn 1976b) across the Manitou Straits Fault: a
previously unnamed lowermost sequence of pillowed
mafic flows, on the order of 8000 m thick, that occurs
southeast of the fault can be traced from Lower Manitou
Lake in the west to beyond Wapageisi Lake in the east.
The name Wapageisi Volcanics is here applied to this se
quence. Correlation has been made between these vol
canic rocks and the lowermost sequence of mafic flows
northwest of the Manitou Straits Fault on lithologic, chemi
cal, and structural grounds (Blackburn 1976b, in prep).
The Wapageisi Volcanics are overlain by a predomi
nantly clastic sequence. West of Taylor Lake this has
been named the Manitou Group (Teal and Walker 1977).
Recent mapping (Blackburn 1976a, 1979a; Teal and
Walker 1977) has shown the group to be composed of a
lower pyroclastic sequence and an upper epiclastic se
quence. Teal and Walker (1977) have documented pas
sage upward from terrestrial to submarine epiclastic fa
cies. Northwest of the Manitou Straits Fault, pyroclastics
of proximal facies at Upper Manitou Lake have been cor
related (Blackburn 1976b) with volcanic rocks of the
Manitou Group. At the east end of the clastic sequence,
abundant magnetite ironstone is intercalated within sand
stone of probable distal turbidite facies at Bending Lake.
Felsic intrusions into the lower, Wapageisi Volcanics, are
subvolcanic phases of some of the more felsic volcanism
in the clastic sequence and may be comagmatic with
phases of the Irene-Eltrut Lakes Batholithic Complex
(Blackburn in prep). Granitoid clasts in conglomerates
(Thomson 1934; Blackburn 1976a, 1979a; Teal and
Walker 1977) of the Manitou Group suggest unroofing of
subjacent batholiths.
The name Boyer Lake Volcanics is given here to a
thick sequence of pillowed mafic flows that lie structurally
above the Manitou Group. The Boyer Lake Volcanics are
intruded by a number of synvolcanic gabbroic sill-like
bodies. Recent investigations (Blackburn in Trowell et al.
1977, 1978) suggest that the Boyer Lake Volcanics are
limited to the north and east by pyroclastic rocks at Ka
washegamuk Lake and south of Melgund Township. They
are bounded in the northwest (Blackburn 1979a) by the
Manitou Straits Fault. Directly across the fault, volcanic
sequences that lie conformably above the pyroclastics of
Upper Manitou Lake are lithologically akin to and continu
ous with Wabigoon Volcanics, and therefore cannot be
correlated with Boyer Lake Volcanics.
Satterly's (1943, 1960) mapping in the vicinity of
Southworth, Satterly, and Melgund Townships indicates
the structural complexity of this area. Lack of detailed
mapping in Avery and MacFie Townships prevents corre
lation at the present time of this structurally complex area
of mafic metavolcanics with the Southern Volcanic Belt of
the Sioux Lookout area. It is noteworthy however that Pal
onen and Speed (1977) have delineated gabbroic intru
sions in the Southern Volcanic Belt east of Sandybeach
Lake, and that magnetic highs similar to those that overlie
these gabbros occur southwestward into MacFie, South
worth, and Avery Townships, and also over the Tobacco
Lake gabbro southeast of Dinorwic Lake. If all of these
gabbros are an integral part of the volcanic stratigraphy
this may indicate the general continuity of volcanic se
quences from the Southern Volcanic Belt southwestward
into the areas mapped by Satterly.
A distinct change in supracrustal rocks occurs
SAVANT LAKE—CROW LAKE
across a sharp faulted contact formed by the Wabigoon
Fault (Satterly 1943; Pettijohn 1939; Blackburn in Trowell
et al. 1977; Blackburn 1979b) along the north shores of
Eagle and Wabigoon Lakes, and the southeast shore of
Sandybeach Lake. Metasediments to the north of this
fault are the along-strike equivalents of metasediments at
Minnitaki Lake, suggesting their inclusion within the Minnitaki Group. Unlike the strata to the south of the fault,
these sedimentary rocks have been tightly folded about
east-trending axes (Blackburn in Trowell et al. 1977;
Blackburn 1979b).
Kakagi-Atikwa Lakes Sub-Area
The Kakagi-Atikwa Lakes sub-area is divided by the
Pipestone-Cameron Fault (Edwards 1976). Correlation of
lithologies across this fault, although suspected, has not
been possible to date.
Southwest of the fault, an east- to north-facing as
semblage is complicated by folding. In the west the lower
part of the assemblage is a thick previously unnamed ho
moclinal, east-facing sequence here called the Snake
Bay Volcanics, composed predominantly of pillowed
mafic flows. South of Kakagi Lake the lower part of the as
semblage is an equally thick, previously unnamed se
quence, here called the Katimiagamak Volcanics, com
posed of predominantly north-facing pillowed mafic flows
that have been extensively intruded by gabbroic sills.
Correlation is made between these two sequences via a
salient of the volcanic belt that lies between Sabaskong
Bay and Whitefish Bay, Lake of the Woods.
Both the Snake Bay and Katimiagamak Volcanics
are overlain by an upper sequence of intermediate pyroc
lastics and metasediments that has been extensively in
truded by differentiated ultramafic to mafic sills (Ridler
1966; Kaye 1974a,b; Davies and Morin 1976). The se
quence was previously unnamed: it is here called the Ka
kagi Lake Volcanics. A number of east-northeast-trend
ing folds occur in this sequence, and have been shown to
post-date emplacement of the sills (Cuddy and Clifford
1972; Schwerdtner et al. 1979. Edwards (in Trowell et al.
1977) has suggested that the central part of Kakagi Lake
is underlain by faults that separate east-trending metavolcanics south of the lake from north-trending metavolcanics north of the lake.
Sedimentary rocks occur at three separate places in
this southern portion of the Kakagi-Atikwa Lakes area: at
Esox Lake, west of Sucan Lake, and at Schistose Lake.
Their stratigraphic equivalence has been demonstrated
by their position above Katimiagamak Volcanics (Ed
wards 1976; Edwards and Sutcliffe 1977). They pass lat
erally westward into metasediments composed of tuffa
ceous debris, to tuff at the base of the pyroclastic
sequence on the south side of Kakagi Lake. This tuff is
shown as tuff-wacke on Kaye's (1974a,b) maps. Similar
"tuff-wacke" occurs higher in the upper pyroclastic se
quence where it strikes north on the north side of Kakagi
Lake. Edwards (in Trowell et al. 1977) has interpreted
them to be one and the same stratigraphic unit that has
been disrupted by the east-trending faults underlying Ka
kagi Lake.
Northeast of the Pipestone-Cameron Fault, complex
folding coupled with lack of detailed mapping in the vicin
ity of Caviar Lake to Lobstick Bay in the northwest, and
Hill Lake in the east, has prevented a complete strati
graphic analysis. However, detailed mapping by Davies
(1973), Kaye (1973), and Edwards (1976), and additional
investigation by Edwards (/nTrowell etal. 1977) suggests
that a lower pillowed mafic flow sequence predominates
in most of the area, and is overlain by a mixed sequence
of intermediate and mafic flows and pyroclastics, and mi
nor felsic flows and tuffs. This upper sequence is discontinuously exposed in synclinal areas at Dogpaw Lake, the
east end of Rowan Lake, east of Hill Lake, and in the vi
cinity of Yoke and Straw Lakes.
A similar sequence is exposed in the core of an anti
cline at Otterskin Lake. A thick, predominantly south fac
ing, sequence of mafic flows lies above it, and is here
named the Brooks Lake Volcanics.
Northward, from Caviar Lake toward Populus Lake,
mapping by Davies and Watowich (1958), Davies (1973),
and Kaye (1973), and additional investigation by Ed
wards (/nTrowell etal. 1977) and Blackburn (/nTrowell et
al. 1978), suggest that tight folding which includes at
least three folds, a syncline flanked on either side by anti
clines, extends northeastward. The name Populus Vol
canics (Davies and Watowich 1958) is extended here to
all these metavolcanics.
It has recently been suggested (Blackburn /nTrowell
et al. 1978) that the large gabbroic intrusion at Mulcahy
Lake is a layered differentiated body that now faces
northwestward. There is meagre information from pillowtop determinations by Davies and Watowich (1958) to
suggest that the mafic metavolcanics that it intrudes also
face northwestward, suggesting that the intrusion is a sill.
As in the Wabigoon-Manitou Lakes area, a distinct
change in supracrustal rocks occurs across a sharp con
tact northwest of the Populus Volcanics. Mapping by Bur
wash (1934) and Davies and Watowich (1958) indicated
predominantly sedimentary rocks, called the Warclub se
ries by Burwash (1934). Extensive felsic metavolcanics
are also present north of Lobstick Bay (Burwash 1934).
Recent work by Edwards (in Trowell et al. 1977) and
Blackburn (/nTrowell etal. 1978) has shown that the met
asediments are tightly folded, and also that further pyroc
lastic rocks are present, particularly at Warclub Lake. The
name Warclub Sediments is used here for this heteroge
neous assemblage of metasediments and metavolcan
ics, with the understanding that it is in all probability stratigraphically equivalent, as suggested by Davies and
Watowich (1958), by direct continuance along strike
northeastward, with metasediments north of Eagle and
Wabigoon Lakes, and further east with the Minnitaki
Group.
General Stratigraphic
Relationships
In any attempt at correlation of stratigraphic sections de
termined for each of the geographic areas discussed in
the previous section, the following two reservations must
be kept in mind. Firstly, the present state of detailed map
ping is such that in many cases individual units have not
yet been traced from one geographic area to the next.
Secondly, sequences are disrupted, both by tectonism
and by batholithic invasion. Sense and amount of move
ment on a number of long faults, e.g. Pipestone-Cameron
Fault, Manitou Straits Fault, Wabigoon Fault, Little Vermi
lion Fault, Miniss River Fault, are not well documented.
Emplacement of large granitic bodies, e.g. Atikwa Bathol
ith, Basket Lake Batholith, Irene-Eltrut Lakes Batholithic
Complex, Lewis Lake-Robinson Lake Batholithic Com
plex, has probably removed voluminous amounts of vol
canic rock by stoping, particularly from the base of indi
vidual portions of the sequence.
However, using certain marker units, and by obser
vation of general stratigraphic sequences, a tentative
correlation has been made throughout the study area
(Table 1).
Five general observations are of paramount impor
tance in making this preliminary correlation. Illustration of
the five general observations is made in Figure 2.
1. Discounting the many reversals due to folding,
doming due to batholithic emplacement, and complica
tions due to faulting, it can be noted that sequences pre
dominantly face inward, toward the centre of the belt. In
particular, around the periphery of the belt, volcanic
rocks near the contact with enclosing batholiths invari
ably face inward. This is the case especially at Kakagi
Lake (adjacent to the Aulneau and Sabaskong Bathol
iths), from Vickers through to Wapageisi Lake (adjacent
to the Irene-Eltrut Lakes Batholithic Complex), from Bluett
Lake through to Sioux Lookout (adjacent to plutonic rocks
of the English River Subprovince), and at Savant Lake,
where the volcanic belt faces inward from the surround
ing plutonic rocks.
2. Where thick stratigraphic sequences commence
at base with a thick succession of mafic flows, these are
situated at the margins of the Savant Lake Crow Lake
belt. Near Sioux Lookout the basal Northern Volcanic
Belt, composed of submarine mafic flows, is situated at
the northern margin of the belt, while in the Manitou-Wabigoon Lakes area, the basal Wapageisi Volcanics are situ
ated at the southern margin. At Kakagi Lake the basal
Snake Bay and Katimiagamak Lake mafic flows are situ
ated at the southwest closure of the belts, while at Savant
Lake the basal Jutten Volcanics are situated at the north
east closure of the belt.
3. Within and away from the margins of the Savant
Lake-Crow Lake belt, highly variable sequences of mafic
to felsic flows and pyroclastics predominate. Where thick
sequences of mafic flows occur in these upper volcanic
units they are mostly towards or at the top of the se
quences. In the Manitou-Wabigoon Lakes area the Boyer
Lake Volcanics, a thick sequence of mafic flows, structur
ally overlies both sedimentary sequences and intermedi
ate to felsic pyroclastics of the Manitou Group, while the
Upper Wabigoon Volcanics are predominantly mafic
flows overlying mixed mafic to felsic metavolcanics. The
mafic flows of the Central Sturgeon Lake Volcanics struc
turally overlie both the North and South Sturgeon Lake
Volcanics, and are therefore at the top of the sequence in
this area. South of Rowan Lake, the Brooks Lake Volcan
ics may overlie the mixed sequence at Rowan Lake, and
therefore be at the top of this sequence.
4. Thick sequences of clastic sedimentary rocks are
associated laterally and vertically with portions of the vol
canic sequences that are highly variable in composition
and texture. In contrast, few sedimentary rocks are asso
ciated with thick sequences of mafic flows, whether those
at the base of sequences, or those towards the top. At
Savant Lake, at Vermilion and Minnitaki Lakes, and in the
Manitou Lakes, much of this clastic sediment has been
shown to be derived by degradation of volcanic edifices
that must have emerged above sea level. In fact, alluvial
sedimentary facies have been documented at Vermilion
Lake (Turner and Walker 1973) and at Manitou Lakes
(Teal and Walker 1977). It is also notable that clastic sedi
mentary units occur predominantly in two zones, as previ
ously noted by Pettijohn (1937, 1972), one near the north
edge of the Savant Lake-Crow Lake belt, and marginal to
the English River Subprovince, and the other more inter
nal, but nearer the south side of the metavolcanic-metasedimentary belt. The former can be traced continu
ously for a distance of 180 km from the vicinity of Sioux
Narrows in the west to Sioux Lookout in the east. Clastic
metasediments at Savant Lake may be considered to be
the eastern extension of these sediments, though sepa
rated by faulting along the Miniss River Fault system. The
latter, internal, zone consists of isolated occurrences at
Kakagi Lake, Schistose Lake, Pipestone Lake, and Esox
Lake, and the more or less continuous 60 km long Mani
tou Lakes sedimentary unit. Metasediments at Raleigh
Lake, southeast of the study area, and those at Sturgeon
Lake are similarly situated internally, but toward the south
side of the belt.
5. Ironstone-bearing formations, predominantly of
oxide facies, occur discontinuously within these two clas
tic sedimentary zones. It is probable that within each
zone these rock-stratigraphic units are correctable and
therefore represent a time-stratigraphic interval. It is also
possible, but quite speculative at this time, that these
chemical sediments were precipitated during the same
time interval in each zone because of their association
with thick sequences of clastic sediments and because
of their apparently similar stratigraphic position.
The authors (Blackburn ei al. 1978) have tentatively
suggested on the basis of these observations that the Sa
vant Lake Crow Lake belt when considered in isolation
shows a degree of bilateral symmetry.
SAVANT LAKE—CROW LAKE
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SAVANT LAKE—CROW LAKE
Preliminary Geochemical
Synthesis
A first evaluation of major element analyses of more than
1000 rock samples taken by the authors supports and
augments the general stratigraphic relationships outlined
above. In parts of the study area analytical work was not
complete at time of writing. We have used 152 analyses
from a previous study by Goodwin (1970) to augment in
formation in those locations. All other analyses either
have been presented in Ontario Geological Survey publi
cations (Edwards 1976, 1978, in prep, Blackburn 1976a,
1979a,c, in prep, Trowell 1974a, 1976, 1977, 1978, in
prep) or will be included in the final report for the present
ongoing project.
Jensen (1976) has shown that a plot of cation per
centages of AI203 , FeO -i- Fe203 -i- TiO2 and MgO, normal
ized to 100 percent (Figure 3) can be used to clearly dis
criminate between suites that he maintains are
characteristic of calc-alkalic, tholeiitic, and komatiitic vol
canism (Figure 4). It should be noted that all three suites
shown on Figure 4 overlap in the region of magnesian
tholeiitic flows (Figure 3). Therefore if the full development
of a particular suite is not present, e.g. high-magnesium
members of the komatiitic suite, or high-iron members of
the tholeiitic suite, difficulty may be encountered in dis
criminating suites. The empirical divider separating highiron tholeiitic basalts from high-magnesium tholeiitic ba
salts provides a convenient reference in such cases.
Plots of samples from the Jutten Volcanics, from the
Northern Volcanic Belt, and from the Wapageisi Volcan
ics are shown in Figure 5. None of these sequences
shows a well developed trend comparable with Figure 4.
However, all three sequences contain samples that fall in
the basaltic komatiite field, and also close to the komati
itic trend as shown on Figure 4. In particular, the Wapa
geisi Volcanics especially indicate this trend. By far the
majority of samples fall in the tholeiitic field, and in all
three cases most are on the high-magnesium side of the
high-magnesium/high-iron divider. All samples analyzed
are from flows. To date no flows with spinifex texture gen
erally considered to be characteristic of true komatiites
(Nesbitt and Sun 1976) have been found in any of the
three sequences. In view of the paucity of samples that
fall in the basaltic komatiite field and absence of spinifex
textures, we prefer to designate these sequences as
magnesian tholeiitic flows (MTF).
Mixed sequences of felsic to intermediate pyroclas
tics and subordinate flows, and mafic flows and subordi
nate pyroclastics are volumetrically the predominant vol
canic assemblages in the study area. Plots for each of
nine sections are given in Figure 6. In three of the sec
tions, namely Lower Wabigoon Volcanics, Rowan Lake,
and Kakagi Lake, supplementary data has been included
from Goodwin (1970), in order to demonstrate the full
range of compositions. On all nine plots samples fall in
both calc-alkalic and tholeiitic fields, but predominantly in
the calc-alkalic field. Only in the case of the Handy Lake
Volcanics (Figure 6) do any samples fall in the komatiitic
field of Figure 3. Almost all triangles show considerable
scatter of data points. A distinct tendency toward the
calc-alkalic trend of Figure 4 is demonstrated in all cases
except Rowan Lake where dacitic to rhyolitic calc-alkalic
* SOUTH AFRICA
•f VITI LEVU, FIJI
SKAERGAARD
A LIQUIDS
A GRANOPHYRE
Rock sampli
{approximate}
MgO
MgO
Figure 3 Classification of subalkalic volcanic rocks by
Jensen cation Plot involving cation percent
ages of AI2O3, FeO + Fe2O3 + TiO2, and MgO
(from Jensen 1976).
Figure 4 Jensen cation plot comparing patterns of vari
ation of komatiitic, tholeiitic, and calc-alkalic
rock suites (from Jensen 1976).
AI 2 0 3
10
rocks appear to be virtually absent, and the Lower Wabi
goon Volcanics where a distinct iron-enrichment trend is
in evidence, with many rhyolites, dacites, and andesites
falling in the tholeiitic field of Figure 3. Because all nine
suites contain samples that plot in the tholeiitic and calcalkalic fields of Figure 3, we designate them as tholeiitic
to calc-alkalic flows and pyroclastics (TCFP).
Plots from five sequences of thick upper mafic flows
are shown on Figure 7. Of these, four (Central Sturgeon
Lake Volcanics, Boyer Lake Volcanics, Upper Wabigoon
Volcanics, Brooks Lake Volcanics) are from the top of se
quences in their respective areas, as noted in the previ
ous section. The fifth sequence, that at Katimiagamak
Lake, is conversely at the base of the sequence in the Ka
kagi Lake area. It is stratigraphically equivalent to basal
sequences at Snake Bay, for which sufficient information
on chemistry is at present not available. The Katimiaga
mak Volcanics are included here because of their similar
NORTHERN VOLCANIC
BELT
chemical signature to the other four sequences. As with
the thick flows at the bases of the sequences (MTF) there
is no well developed trend comparable with Figure 4. In
contrast to MTF sequences, samples that fall in the komatiitic field are only found in the Boyer Lake Volcanics (one
sample) and the Katimiagamak Volcanics (one sample).
In similarity to MTF sequences, by far the majority of sam
ples fall in the tholeiitic field, but in contrast to MTF se
quences in all five cases most are on the high-iron side of
the high-magnesium/high-iron divider. Also in contrast to
MTF sequences there is a distinct tendency toward iron
enrichment. Because no distinct tholeiitic trend, as indi
cated on Figure 4, is present we designate these assem
blages as Fe-tholeiitic flows (FTF) rather than high iron
tholeiites as per Jensen's (1976) classification.
Composite plots of all 1191 points (Figure 8) further
emphasises the tripartite division of the three suites, and
also their overlap in the vicinity of the magnesian tholeiitic
field.
JUTTEN VOLCANICS
100 POINTS
FeO + P62O3 + TiOo
AI2O3
MgO
WAPAGEISI VOLCANICS
Figure 5 Jensen cation plot for Jutten Volcanics, Northern Volcanic Belt and Wapageisi Volcanics, showing their tholeiit
ic, relatively magnesian, character.
11
SAVANT LAKE—CROW LAKE
Correlation of Geochemistry
With Stratigraphy
Regional
The distribution of the three types of volcanic suites de
scribed in the previous section is shown on Figure 9.
Comparison of Figure 9 with Figure 2 indicates lower
mafic flow sequences are tholeiitic and, apart from Kati
miagamak Lake where they are predominantly Fe-tholeiitic, are predominantly magnesian (though generally less
than 10 weight percent MgO). Middle mixed sequences
of Figure 2 are highly variable, from tholeiitic to calc-alkal
ic, and in general show a distinct calc-alkalic trend. Up
per mafic flow sequences are predominantly Fe-tholeiitic.
It has been suggested by Goodwin (1968) that Ar
chean "greenstone" belts are characterised by a general
progression upwards in sequences from a basal basaltic
flow "platform" through an intermediate andesitic to dacitic, predominantly pyroclastic, stage, to eruption of rhyolites, the latter phases constituting an emergent island
154 POINTS
(82 FROM GOODWIN, 1970)
LOWER WABIGOON
VOLCANICS
ROWAN LAKE
47 POINTS (24 FROM
GOODWIN, 1970)
TiO2
98 POINTS
30 POINTS (18 FROM
GOODWIN, 1970)
KAKAGI LAKE
AI2O3
MgO
MANITOU SECTION
Figure 6 Jensen cation plots for Rowan Lake Volcanics, Kakagi Lake Volcanics, Lower Wabigoon Volcanics, Manitou
Lakes section, North and South Sturgeon Lake Volcanics, Handy Lake Volcanics, and Beckington Road and
Morgan Island sections of the Northeast Arm Volcanics showing their calc-alkalic to tholeiitic character.
12
fore rests on a single section, that at Snake Bay-Kakagi
Lake. The present study does not confirm this four-fold
subdivision to prevail throughout the Savant Lake Crow
Lake area. Tentatively, a broad three-fold subdivision is
suggested here although the superposition of thick Fetholeiitic flows above the tholeiitic to calc-alkalic flows
and pyroclastics is at least in part due to faulting; in the
Manitou Lakes area, Blackburn (1976b, in prep.) has
suggested that the Boyer Lake Volcanics are thrust on
top of the Manitou Group metasediments and pyroclas
tics, and may be the lateral equivalents of Wapageisi Vol
canics.
"edifice" stage. In northwestern Ontario, Wilson et al.
(1974) have suggested that a four-fold subdivision of vol
canic sequences is in evidence, namely a lower basic,
middle basic, middle felsic, and an upper cyclic. This
analysis was based essentially on two cross-sections,
one from Snake Bay upward through the Kakagi Lake se
quence, and a second from Wapageisi Lake upward
through the Stormy Lake succession, to Kawashegamuk
Lake. Although their Snake Bay-Kakagi Lake section is
entirely valid, that at Wapageisi-Kawashegamuk Lake is
complicated by a major synclinal fold axis not recognized
by them (Blackburn 1976b). Their generalization there
HANDY LAKE VOLCANICS
69 POINTS
NORTH STURGEON LAKE
VOLCANICS
72 POINTS
79 POINTS
NORTHEAST ARM VOLCANICS
(BECKINGTON ROAD SECTION)
AI 20 3
SOUTH STURGEON LAKE
VOLCANICS
MgO
NORTHEAST ARM VOLCANICS
(MORGAN ISLAND SECTION)
13
SAVANT LAKE—CROW LAKE
Local
The greatest chemical variations in the study area are
shown by the above geochemical synthesis to be in the
TCFP sequences. Much of this is due to multiple tholeiitic
to calc-alkalic cycles. Such can be shown to be the case
for example at Sturgeon Lake (Trowell in prep, Franklin et
BROOKS LAKE
VOLCANICS
al. 1977). To illustrate this elsewhere in the study area we
have chosen a section through TCFP and overlying FTF
at Wabigoon Lake (Figure 10). This portion of the northfacing homoclinal sequence is divisible on a chemical
basis into nine units (numbered 1 to 9 from base to top).
Each of the fields are distinct. The cyclical nature of
the volcanism is evident, with progressive enrichment in
UPPER WABIGOON
VOLCANICS
34 POINTS (28 FROM
GOODWIN, 1970)
61 POINTS
FeO -i- F02O3 * TiO2
70 POINTS
AI2O3
MgO
CENTRAL STURGEON LAKE
VOLCANICS
BOYER LAKE
VOLCANICS
KATIMIAGAMAK VOLCANICS
Figure 7-^ensen cation plots for Brooks Lake Volcanics, Katimiagamak Volcanics, Boyer Lake Volcanics, Upper Wabi
goon Volcanics, and Central Sturgeon Lake Volcanics showing their tholeiitic, relatively iron-rich, character.
14
iron with each successive pulse of mafic magma. Within
TCFP possibly three cycles can be recognized: 1 through
3; 4 through 5; and 6 through 8. Unit 9 is distinctively
higher iron tholeiite than preceding phases, and may rep
resent the base of a fourth, overlying cycle within FTP.
It should be noted that some of these chemically defi
ned units correspond to distinct physically defined units.
Basaltic units 1, 4, 6, 7 and 9 are flows; more felsic units
2, 3, 5 and 8 are predominantly pyroclastic. Paralleling
iron enrichment, basaltic flows become more distinctly
FeO + F62O3 4- TiO2
MgO
MTF
260 POINTS
FTP
226 POINTS
TCFP
705 POINTS
Figure 8—Composite Jensen cation plot of 1191 samples from the Savant Lake—Crow Lake area comparing the chemi
cal compositions of the three volcanic suites.
MAGNESIAN THOLEIITIC FLOWS (MTF)
THOLEIITIC TO CALC-ALKALINE FLOWS
AND PYROCLASTICS (TCFP)
FE-THOLEIITIC
FLOWS (FTF)
SEDIMENTS
N
FAULTS
^*"*
O
IRON FORMATION
50
100 KM
CROW
(KAKAGDTAKE
Figure 9—Sketch map to show distribution of the three volcanic suites in the Savant Lake—Crow Lake area.
15
SAVANT LAKE—CROW LAKE
pillowed, the pillows larger in size, and inter-pillow mate
rial more prominent.
Approach to a Tectonic Model
In preceding sections it has been shown that geochemi
cal analysis supports and augments the stratigraphic
synthesis of the volcanic-sedimentary units. Subjacent
granitic batholiths are an integral part of the structural
complexity. Although it remains to be shown in detail to
what extent their emplacement has deformed the supra
crustal rocks, it has been suggested at a number of
places (Blackburn 1979a, in prep, this study; Edwards
1978; Trowell 1974a) that local shallow level intrusive
phases of batholiths have erupted at the surface, and
particularly during TCFP volcanism. Conversely, nowhere
within the study area have volcanic rocks been shown to
FeO * Fe2 O3 -i- TiO2
RHY.
AI 2 0 3
\
\ D AC A AND.\
BAS
MgO
Figure 10—Section through tholeiitic to calc-alkalic flows and pyroclastics (TCFP) and overlying Fe-tholeiitic flows (FTP)
at Wabigoon Lake. Sample traverse shown as heavy line. Portions of Jensen cation diagrams show fields for
units 1 to 9, with the following number of samples per unit: 1-26, 2-7, 3-5, 4-4, 5-5, 6-6, 7-7, 8-9, 9-6.
16
N
—— ENGLISH——
WABIGOON SUBPROVINCE
RIVER
SUBPROVINCE
KAKAGI-SAVANT LAKES
GREENSTONE BELT
Figure 11—Cross-section illustrating hypothetical stage of development during time of late tholeiitic to calc-alkalic flow
and pyroclastic (TCFP) volcanism. MTF indicates magnesian tholeiitic flows; crosses indicate two phases of
granitic intrusions.
lie on a granitic basement. However, there is considera
ble evidence that batholithic emplacement commenced
early in the evolutionary history as shown by the graniteclast conglomerates that unconformably overlie MTF,
lowermost, Jutten Volcanics at Savant Lake. Similarly,
granitic clasts are present in uppermost conglomerates
in the Manitou Group.
Significantly, the presence of MTF, in all cases at the
base of sequences, discontinuously along the northern
and southern edges of the belt, combined with its great
thickness, in places on the order of 10 000 m, suggests
its earlier continuity, possibly beneath the belt. Thin pillow
rims, general absence of amygdules and hyaloclastite,
leads us to interpret them as deep-submarine, probably
fissure outpourings. Also characteristic are plagioclasephyric mafic flows, some of which, for example in the
Manitou-Stormy Lakes area, can be traced for tens of ki
lometres along strike. Over a protracted period, bathol
ithic invasion concomitant with crustal downwarping
would have removed much of this sequence by stoping
while at surface calc-alkalic volcanism produced island
edifices (Figure 11).
Reference to tectonic models presented in the litera
ture (e.g. Anhaeuser 1975; Glikson 1978; Gorman et al.
1978; Young 1978; Burke et al. 1976; Baragar and
McGlynn 1976, 1978; Goodwin and West 1975; Talbot
1973) leads us to suggest that absence of a recognizable
granitic or gneissic basement upon which the lowermost
mafic volcanic rocks can be shown to have been laid
down is not inconsistent with a mobilist or plate tectonic
model. Such a model would account for crustal down
warping, such that MTF sequences on either side of the
belt might represent elements of opposing oceanic
plates. Langford and Morin (1976) have speculated on a
plate tectonic model for this part of Superior Province
based primarily on lithochemical data.
Voluminous sediments derived by degradation of
volcanic piles and emerging batholiths were deposited
within both what is now the Wabigoon Subprovince and
northwards within what is now the margin of the English
River Subprovince.
The presence of mafic tholeiitic volcanism structur
ally at the top of some of the sequences is not as yet un
derstood. Its present distribution within the belt, either in
the cores of synclines, or terminated against faults, sug
gests it may have formerly been more continuous. In the
17
SAVANT LAKE—CROW LAKE
Manitou Lakes portion of the area Blackburn (1976b) has
suggested that Boyer Lake Volcanics, of FTP affinity,
have been technically emplaced, along a thrust decolle
ment, above metasediments and pyroclastics of the Man
itou Group. Such an interpretation is not inconsistent with
plate tectonic theory, which emphasises dominance of
horizontal shortening over vertical tectonics (Burke era/.
1976).
Many of the FTP sequences, unlike MTF sequences,
are amygdaloidal, suggesting a shallow submarine envi
ronment, and they are rarely plagioclase-phyric. These
characteristics, in conjunction with their different chemis
try, suggest that they are not lateral equivalents of lower
most MTF sequences, but may have originated in a differ
ent geochemical environment. McMaster (1978) has
suggested from trace element data that lowermost (MTF)
Wapageisi Volcanics in the Manitou-Stormy Lakes portion
of the area are of ocean-floor affinity.whereas Boyer Lake
Volcanics (FTP) are of island-arc or back-arc-basin affi
nity. These conclusions are also not inconsistent with
plate-tectonic theory.
shear folding associated with movement along the Stur
geon Narrows Structural Zone may have masked initial
association between these gold occurrences and vol
canic stratigraphy.
Production at the St. Anthony mine was from a de
posit within granitic rocks that intrude the Northeast Arm
Volcanics (Trowell 1977, in prep).
Gold mineralization at the Darkwater mine is found in
quartz veins in the Beidelman Bay Pluton, which appears
to be a subvolcanic felsic intrusion (Trowell in prep).
Sioux Lookout Sub-Area
Gold in the Savant Lake area (Bond 1977, 1978, 1979)
occurs in quartz veins situated throughout the Jutten and
Handy Lake Volcanics.
In the Sioux Lookout area the preponderence of gold oc
currences are in the Central Volcanic Belt. Many are
associated with hypabyssal, probably subvolcanic intru
sions while several, for example the Newlund or Goldlund
deposit (Webb 1948; Speed 1978; Page 1979), appear to
be associated with granitoid intrusions that may be either
superimposed on volcanic stratigraphy or of subvolcanic
origin. It is of interest that a northeast-trending zone of
'spherulitic lavas' (Webb 1948; Armstrong 1951) occurs
at the same approximate stratigraphic level as, and in
close proximity to, the Goldlund deposit (Webb 1948;
Armstrong 1951) and past explored ground to the east
(Armstrong 1951; Chisholm 1951). Examination of these
'spherulitic lavas' (Trowell 1977; Reid 1978) indicates that
some of them are variolitic lavas containing felsic varioles
possibly of immiscible origin (Gelinas et al. 1976). Data
are not available but felsic varioles may be preferentially
enriched in gold with respect to the matrix or the average
abundances of gold in igneous rocks.
Three gold occurrences in the northeast extension of
the Central Volcanic" Bejt occur at the same stratigraphic
level in mafic metavolcanics (Page 1978b). Gold here oc
curs in quartz veins accompanied by carbonate and sul
phides (pyrite-l-galena sphalerite chalcopyrite) (Page
1978b). These occurrences may be time-equivalent and
possibly related to emplacement of the intrusion, proba
bly subvolcanic, at Clamshell Lake (Page 1978b).
A gold-silver occurrence on Vermilion Lake (Eimiller
Claims, Johnston 1972) is situated along the probably
secondarily silicified contact between quartz porphyry of
subvolcanic origin to the south and tuff and conglomerate
to the north. It is possible that this contact was actually an
erosional unconformity and that residual placer gold was
subsequently concentrated during silicification of this
zone.
Sturgeon Lake Sub-Area
Wabigoon-Manttou Lakes Sub-Area
Gold along the Northeast Arm of Sturgeon Lake similarly
occurs in quartz veins. Here, however, shearing and
Gold deposits mostly in quartz veins occur in the EagleWabigoon Lakes area along a specific horizon, distinctly
related to felsic volcanism, and associated subvolcanic
plutonism. At Eagle Lake numerous occurrences and
prospects (Moorhouse 1941) are located either within or
peripheral to a lobe of the Atikwa Batholith. One of these,
the Baden Powell mine, is located well within the granitic
phase of the batholith. Other gold occurrences northeast
of Meridian Bay are within felsic flows and tuffs. Field in
vestigation during the course of this study has shown that
Mineral Deposits1
Gold
Three broad categories of gold occurrences can be rec
ognized in the area: 1) those tied to volcanic and subvol
canic stratigraphy, very often the same stratigraphy as
suggested for base metal deposits and (subvolcanic)
porphyry copper and molybdenum deposits, respec
tively; 2) those occurrences associated with later felsic in
trusions that possibly intrude volcanic stratigraphy; and
3) those occurrences situated within quartz veins having
no apparent relationship to volcanic activity or igneous in
trusions. Individual occurrences often combine features
of more than one class.
Savant Lake Sub-Area
1 Locations of specific deposits discussed in this section can be
found in Compilation Maps 2115 (Davies and Pryslak 1967),
2169 (Davies et al. 1970), and 2175 (Ferguson et al. 1970), the
Ontario Mineral Map 2310 (ODM 1974), and in reports by Go
odwin (1965), Beard and Garratt (1976), and Breaks et al.
(1978). Maps 2115,2169 and 2175 are currently being revised.
18
there is a transition from granitic rocks through to felsic
flows in this location and that this lobe of the batholith is a
subvolcanic phase.
Further east, on the west side of Wabigoon Lake, nu
merous gold occurrences and prospects (Satterly 1943)
occur at the same stratigraphic level as those at Eagle
Lake. Two past producers, the Bonanza mine and the Re
deemer mine are located here. Other gold occurrences
are at Contact Bay of Wabigoon Lake, where the Dor6
Lake lobe of the Atikwa Batholith may be a subvolcanic
source of felsic volcanism.
In the Manitou Lakes, numerous gold occurrences
and prospects (Thomson 1934, 1942; Blackburn 1976a,
1979a,c) are located principally in quartz veins associ
ated spatially with calc-alkalic pyroclastic volcanism
northwest of the Manitou Straits Fault. Three past produc
ers, the Laurentian, Elora, and Big Master mines are all lo
cated at Trafalgar Bay of Upper Manitou Lake, at the tran
sition from underlying calc-alkalic pyroclastic volcanism
to overlying mixed tholeiitic to calc-alkalic flows and py
roclastics. Earlier interpretations (Thomson 1934, 1936,
1942) related the mineralization to intrusion of felsic
dikes, and to association of a structural "break". More re
cently Blackburn (1979a) has suggested that the felsic
units are flows and therefore that the gold is genetically
associated with the volcanism.
A number of occurrences and prospects north of Kawashegamuck Lake are spatially associated with recently
identified felsic volcanism and a zone of intense carbona
tization (Blackburn in Trowell et al. 1977; Blackburn
1979d). The only past producer, the Sakoose (Golden
Whale or Van Houten) mine reportedly developed on a
quartz-feldspar porphyry intrusion in mafic metavolcanics (Thomson 1934), occurs stratigraphically immediately
below a thick sequence of proximal felsic pyroclastic
breccia and associated tuff, suggesting a volcanic asso
ciation.
Kakagi-Atlkwa Lakes Sub-Area
At Straw Lake, in the vicinity of Pipestone Lake, gold was
produced from the Straw Lake Beach mine, located in fel
sic metavolcanics (Edwards in prep, Edwards in Trowell
et al. 1977). Near Sioux Narrows, gold was produced
from the Regina mine, located in quartz veins associated
with altered mafic rocks adjacent to a small granitic stock
(Fraser 1945; Burwash 1934; Edwards in Trowell et al.
1977). It is possible that the stock was either the source
for or concentrated the gold.
Other abundant occurrences and prospects in the
Kakagi-Rowan Lakes area are in quartz veins scattered
throughout the mafic to felsic volcanic sequences, with
little apparent stratigraphic control. Gold also occurs withcopper mineralization at the Maybrun mine and the Em
pire mine, both in mafic metavolcanics, in the vicinity of
Atikwa Lake (Davies 1973).
Base Metals
Base metal mineralization occurs primarily in three gen
eral environments in the area: 1) directly associated with
volcanism; 2) associated with subvolcanic and granitoid
plutons; and 3) associated with mafic and ultramafic in
trusions and flows.
Volcanogenic Base Metal Sulphides
Sturgeon Lake Sub-Area
Mattabi Mines Limited and Sturgeon Lake Mines Limited
are the only active producers of Zn, Cu, Ag, and Pb in the
Crow Lake Savant Lake area. Two further deposits
await development (Table 2).
TABLE 2 SUMMARY OF BASE METAL SULPHIDE DEPOSITS IN THE STURGEON LAKE AREA. DATA FROM FRANKLIN ET AL.
(1977).
NAME
COMPANY
DISCOVERY
DEPOSIT TYPE
CURRENT
ZN
CU
AU
PB
AG
"/o
"/o
DATE
TONNAGE
"/o
OZ/T
OZ/T
ESTIMATE
(TONS)
Zn-Cu-Ag-Pb
Mattabi mine
Mattabi Mines
0.8
Sept. 1969
7.5
0.77
3.10
136658002
Boundary mine
Lyon Lake and
Creek deposits
Ltd. 1
Sturgeon Lakes
Mines Ltd. 1
Mattagami Lake
Mines Ltd.
Oct. 1970
Zn-Cu-Ag-Pb-(Au)
Oct. 1971 8. Feb. Zn-Cu-Ag-Pb
21105842
10.64
2.93
1.47
6.14
4 029 5002
6.66
1.15
0.63
3.3
0.021
1972
1 Producer.
2 All tonnage figures are pre-production estimates.
19
SAVANT LAKE—CROW LAKE
All four deposits are in the South Sturgeon Lake Vol
canics. They occur near the top of the Darkwater and
Lyon Lake Volcanic Cycles (Trowell 1977, in prep).
The deposits are conformably situated within inter
mediate to felsic volcanic breccias. The breccias are
dominantly redeposited debris flow deposits, though in
the immediate mine areas monolithic felsic breccias
could have formed in-situ by autobrecciation of felsic do
mes. The breccias are overlain by mafic metavolcanic
flows, locally pillowed and coarsely amygdaloidal. Car
bonaceous shales occur at approximately the same stra
tigraphic level as the sulphides and in some cases could
be the lateral equivalents of the deposits. The immediate
footwall rocks of these deposits are variably altered
(Franklin et al. 1975; Hinzer 1977; Trowell in prep). As
well, a widespread pervasive alteration of the breccias
below the ore-bearing horizons has occurred (Lavin
1976). East of O'Briens Landing an epizonal subvolcanic
intrusion, the Beidelman Bay Pluton, is situated within the
base of the breccia pile and has many of the characteris
tics of porphyry copper systems (Trowell 1974a; Priske
1974; Franklin et al. 1977).
According to Hodgson and Lydon (1977), the main
requirements for a hydrothermal system are an aquifer
zone, a heat source, a caprock unit, and recharge and
discharge channels. The breccia pile not only satisfies
the requirement of an aquifer but also could be the
source of the metallic elements. The Beidelman Bay Plu
ton acted as a heat source and, as well, probably pro
vided various volatiles that aided in the leaching of and
the transporting of the metallic elements as complex ions
during a period of resurgent or second-boiling activity.
The anomalous chemistry of the Darkwater Lake Cycle
(Trowell in prep) could indicate that a self-sealing cap
formed as a result of boiling of the discharge fluids as
they rose through the breccia pile. Some of the interca
lated mafic metavolcanic flows could have acted as rela
tively impermeable barriers confining the fluids circulat
ing through the breccias. The monolithic autoclastic
breccias could represent the explosive eruption products
that would result from boiling of the discharge fluids. Dis
charge channels are likely indicated by the alteration
zones present beneath the deposits themselves.
As indicated by the coarse amygdules in the overly
ing flows, and the carbonaceous shales, deposition of the
metallic elements appears to have occurred in relatively
shallow water on the sea-floor, probably in a restricted
quiescent environment, and possibly under biogenic
controls.
Savant Lake Sub-Area
Similarities between the South Sturgeon Lake Volcanics
and the Handy Lake Volcanics of the Savant Lake area
make the latter a favourable prospecting target for vol
canogenic base metal sulphide mineralization.
North of the town of Savant Lake two base metal oc
currences are situated within redeposited volcanic py
roclastics and volcanogenic metasediments of the Handy
Lake Volcanics (Table 3). The occurrences have been in
terpreted to be distal facies with a possible source to the
west (Trowell 1978). The Hadley occurre/ice is a small
pod of base metal sulphides, possibly a portion from a
larger base metal sulphide body, that was detached from
the main body and deposited in its present position.
Both the Darkwater Lake and Claw Lake fragmentals
of the South Sturgeon Lake Volcanics (Trowell in prep)
and this section of the Handy Lake Volcanics plot domi
nantly in the calc-alkalic field on a cation plot (Jensen
1976). Kyanite and andalusite that occur in the altered
footwall rocks at the Mattabi mine are also found within
the Handy Lake Volcanics northwest of Evans Lake. This
development of peraluminous units may be the result of
leaching of the other major elements by an active hy
drothermal system, the development of specific alumino
silicate minerals being the result of superimposed meta
morphism.
On and to the west of Highway 599, north of the town
of Savant Lake, coarse breccias of redeposited and py
roclastic origin are locally intensely carbonatized (Bond
1978); a similar carbonate alteration zone is developed in
proximity to the Mattabi mine (Franklin era/. 1977).
Possible epizonal subvolcanic phases now intruded
by late granitoid phases of the Lewis Lake Batholith
(Breaks and Bond 1979) occur marginal to the fragmen-
TABLE a BASE METAL SULPHIDE OCCURRENCES IN THE SAVANT LAKE AREA (HANDY LAKE VOLCANICS).
OCCURRENCE
Savant
Occurrence
Hadley
Occurrence
20
HOST ROCKS
METALS
Cu-Zu-Pb-Ag Handy Lake Volcanics
metasediments and
intermediate tuffs
Zn-Pb-AgHandy Lake Volcanics
intermediate tuffs
(Cd)-(Au)
MINERALIZATION
Disseminated pyrite, chal
copyrite, sphalerite, galena,
minor pyrrhotite
Bands and patches of mas
sive sphalerite and galena
and minor chalcopyrite
ASSAY DATA
1.670/0 Cu, 1.4407o Zn, Q.28% Pb, 3.46 oz.
Ag/ton over width of 3 m (Shklanka, 1969)
21.8 07o Zn, 8.850Xo Pb, U.08% Cd, 1.88 oz.
Ag/ton, 0.01 oz. Au/ton over 1.2 m (File
63.2892, Cam Mines Ltd., Assessment
Files Research Office, Ontario Geological
Survey, Toronto)
tals near the town of Savant Lake. Like the interpreted
role played by the Beidelman Bay subvolcanic pluton
within the South Sturgeon Lake Volcanics, this now dis
rupted subvolcanic body could have played the role of
heat source in the development of a hydrothermal system
within the Handy Lake Volcanics.
The search for base metal sulphide mineralization in
the Handy Lake Volcanics may be complicated by the
high metamorphic grade and accompanying metasoma
tism (Bond 1978; Trowell 1978; Lefebvre etal. 1978) and
by the complex folding. Both the Savant and Hadley oc
currences contain anomalously high mercury values (up
to 1580 ppb), and the Savant occurrence contains high
tin values (up to 650 ppm) indicating that lithogeochemi
cal prospecting methods might aid in delimiting possible
areas of major base metal mineralization.
Sioux Lookout Sub-Area
In the Sioux Lookout area intermediate and felsic volcanic
breccias with possible hypabyssal equivalents occur on
Vermilion Lake (Trowell 1978). The hypabyssal phases
are locally extensively intruded by quartz-tourmaline
veins. As well they are quite sericitic and locally pyritic,
possibly reflecting original hydrothermal alteration. The
breccias themselves are coarse, possibly near-vent de
posits, and are locally set in an iron carbonate matrix of
chemical sediment origin (Trowell 1978). Examination of
these breccias, and their western extension into the
Bluett Lake area (Breaks and Bond 1975; Page 1979) is
warranted.
Felsic and intermediate fragmentals, flows, and pos
sible hypabyssal equivalents occur east of Sioux Lookout
in the area of Superior Junction (Johnston 1972; Trowell
1977) and extend to the northeast (Page 1978b). A cop
per occurrence is known at Allan Lake, south of Superior
Junction (Johnston 1972), and the Rosnel occurrence,
hosted by carbonatized quartz-sericite schist, comprises
disseminated pyrite, chalcopyrite, and sphalerite (Page
1978b).
Other areas near Sioux Lookout that perhaps warrant
further exploration are a newly defined zone of intermedi
ate fragmentals situated at Southeast Bay, Minnitaki Lake
(Bartlett in Trowell et al. 1978), and intermediate to felsic
breccias in the Pickerel Arm area of Minnitaki Lake (John
ston 1969; Palonen and Speed 1977; Trowell in Trowell et
al. 1978).
Wabigoon-Manitou Lakes Sub-Area
At Eagle and Wabigoon Lakes felsic to intermediate frag
mentals and flows occur toward the top of the lower
mixed felsic to mafic sequences. This zone was early re
cognised as favourable for gold occurrences, but its po
tential for Cu-Zn-Pb mineralization associated with proxi
mal volcanic activity is also important. However, in spite
of exploration, little mineralization of this kind has been
reported to date.
At the north end of Meridian Bay of Eagle Lake, in the
vicinity of Fornieri Bay, chalcopyrite has been reported in
both surface sampling and a number of drill holes. Disse
minated sulphides with associated gold mineralization
are present over a considerable area in rhyolitic flows
and tuffs. In a report for Kamlo Gold Mines Limited (As
sessment Files Research Office, Ontario Geological Sur
vey, Toronto) the values of copper in the best two grab
samples taken were reported to be 0.44 percent and 0.72
percent. A copper assay of 0.76 percent was also re
ported over a 5-foot length in one drill hole in a sample
taken from a 50-foot section that assayed an average of
0.432 percent Cu. Other drill holes on the property inter
sected chalcopyrite in small amounts. Considerable min
eral exploration (Assessment Files Research Office, On
tario Geological Survey, Toronto) southward from Fornieri
Bay to Meridian Bay has shown the presence of iron sul
phide and oxide minerals generally in mafic flows, while
at Buchan Bay, to the east, exploration has outlined mag
netite-rich zones that may be along-strike equivalents. To
date, no economic mineralization has been discovered
but this zone is suggested for further exploration.
Moorhouse (1941) outlined a sequence of mixed fel
sic and intermediate flows and pyroclastics that extend
from Fornieri Bay in the west across Eagle Lake to Spring
Bay in the east. Later mapping by Satterly (1943) deli
neated similar lithologies along strike to the east, extend
ing across Wabigoon Lake to Daunais Bay. Considerable
prospecting and exploration has been carried out along
this zone, in the past predominantly for gold. Because of
its felsic pyroclastic nature, it is suggested here that it is
also potentially favourable for volcanogenic base metal
(Cu-Pb-Zn) deposits. In addition, the presence of rhyolitic
rocks somewhat lower in the section, near Contact Bay of
Wabigoon Lake, suggests proximity of a felsic centre of
volcanism.
Further to the southeast, between Melgund Town
ship and Kawashegamuk Lake, investigation by the pres
ent workers (Blackburn in Trowell et al. 1977) has iden
tified felsic pyroclastic and flow rocks in the vicinity of
Church Lake that were not outlined in earlier mapping
and compilation (e.g. Davies and Pryslak 1967). Explora
tion in recent years in this area (Assessment Files Re
search Office, Ontario Geological Survey, Toronto) has
been extensive (Beard 1975; Beard and Rivett 1977,
1978; Beard and Scott 1976), and minor amounts of CuZn mineralization have been found (Blackburn 1979d).
In the Manitou Lakes portion of the area Blackburn
(1976a, 1977a, 1979a, in prep, /nTrowell et al. 1977) has
suggested a number of situations suitable for base metal
exploration. These include proximal felsic to intermediate
pyroclastics and flows and clastic sedimentary rocks,
spatially associated with felsic porphyries that intrude the
calc-alkalic sequences (Blackburn 1977b), in particular
at Frenchman Island of Upper Manitou Lake, at Sunshine
Lake, and at Thundercloud and Washeibemaga Lakes.
Kakagi-Atikwa Lakes Sub-Area
Felsic porphyries that intrude and are subvolcanic equiv
alents of calc-alkalic volcanic rocks are also present at
Esox Lake and at Dash Lake in the vicinity of Pipestone
21
SAVANT LAKE—CROW LAKE
Lake. Because these bodies define centres of felsic vol
canism, they represent good exploration targets for vol
canogenic base metal sulphides, as discussed by Ed
wards (1976, 1978, in prep) and by Beard and Scott
(1976).
At Kakagi Lake Cu-Zn-Ag mineralization has been
discovered in dacitic tuff south of the Stephen Lake plu
ton (Davies and Morin 1976). These tuffs can be traced a
considerable distance along strike around fold structures
north of Kakagi Lake, and are possibly continuous with
units called tuff-wacke (Kaye 1974a,b; Edwards 1976)
and waterlain tuff (Edwards 1976) along the south side of
Kakagi Lake. The correlation increases the potential tar
get area for base metal sulphides.
Northeast of the Pipestone-Cameron Fault, the upper
mixed mafic-felsic sequences in synclinal structures at
Yoke, Hill, Rowan and Dogpaw Lakes have been sug
gested by Edwards (in Trowell et al. 1977) to be poten
tially favourable for volcanogenic base metal sulphide
mineralization.
Copper and Molybdenum Deposits Associated
with Subvolcanic and Granitoid Plutons
Several of the porphyritic epizonal subvolcanic plutons
that occur throughout the area contain disseminated cop
per and molybdenum (and gold) mineralization. As well,
later granitoid plutons contain disseminated molybde
num mineralization.
Savant Lake Sub-Area
At Savant Lake porphyritic hypabyssal trondhjemite
phases marginal to the Handy Lake Volcanics (Bond
1978) could represent the remains of an epizonal intru
sion^) now extensively intruded by granitoid phases of
the Lewis Lake Batholith (Breaks in prep). Minor amounts
of chalcopyrite were observed in these rocks (Trowell
1977) where they have been newly exposed by the re
cently constructed Marchington Road.
Sturgeon Lake Sub-Area
Copper and molybdenum mineralization occur in the Beidelman Bay Pluton at Sturgeon Lake. A possible coeval
and comagmatic intrusion, the Shanty Lake Pluton (Tro
well 1970; in prep) contains disseminated molybdenite
with minor chalcopyrite. The Beidelman Bay Pluton has
several features characteristic of 'porphyry copper' sys
tems (Trowell 1974a; Priske 1974; Franklin era/. 1977),
and gold mineralization (see "Gold") at the Darkwater
mine (Horwood 1938b, Trowell 1974a) could also be of
porphyry affinity.
Sioux Lookout Sub-Area
At Sioux Lookout a composite trondhjemite-quartz diorite-diorite stock situated in the Northeast Bay of Minnitaki
Lake may be comagmatic to, and a subvolcanic intrusion
associated with, the Central Volcanic Belt (Johnston
1972;
22
Page and Clifford 1977, Page 1978a). Copper and cop
per-molybdenum occurrences are found within the dioritic phases. A similar pluton situated at David Lake to the
north contains no reported mineralization.
A porphyritic felsite intrusion on the south shore of
Vermilion Lake contains a copper occurrence set in an
enclave of volcanic-clast conglomerate.
Copper mineralization is reported in a mafic metavolcanic enclave in a porphyritic body situated at the east
entrance to Pickerel Arm, Minnitaki Lake (see Colvine and
Sutherland 1979, for detailed discussion of this area).
Along the margin of the Lateral Lake Stock several
molybdenite occurrences occur in late quartz and peg
matite veins. The descriptions of these occurrences have
been summarized by Colvine and McCarter (1977) and
Page (1979).
Kakagi-Atikwa Lakes and Wablgoon-Manitou Lakes SubAreas
Molybdenite occurrences have been located at a few
scattered occurrences at the edge of the Dor6 Lake lobe
of the Atikwa Batholith. One of these is near Contact Bay
of Wabigoon Lake (Assessment Files Research Office,
Ontario Geological Survey, Toronto) and two others are in
the Manitou Lakes area (Blackburn 1976a, 1979c). The
occurrences are in pegmatite veins both within the grani
tic rocks of the batholith and within adjacent metavolcanics. Minor occurrence of molybdenite is reported in drill
core (Assessment Files Research Office, Ontario Geolog
ical Survey, Toronto) from near Mennin Lake, adjacent to
the Revell Batholith.
Molybdenite has also been found associated with
gold in quartz veins and quartz-feldspar porphyry dikes
that intrude mafic metavolcanics at Wapus Lake north of
Kakagi Lake (Davies and Morin 1976). The porphyry
dikes appear to be part of an irregularly shaped felsic
porphyry intrusion centred on Wapus Lake.
Molybdenite associated with copper has been re
ported from gold-bearing quartz veins adjacent to the
Stephen Lake pluton, north bf Kakagi Lake (Davies and
Morin 1976). However, this has not been subsequently
substantiated.
Copper and Nickel in Mafic and Ultramafic
Intrusions and Flows
Savant Lake Sub-Area
At Savant Lake, metamorphosed ultramafic intrusions,
ranging from peridotite to pyroxenite in composition, are
situated within the lower Jutten Volcanics at Armit Lake
(Hudec 1965; Sutcliffe in Trowell et al. 1977). An ultra
mafic flow overlies granitoid-clast conglomerate in the
upper eastern portion of Savant Lake. Two anthophyllite
flows of apparent ultramafic affinity are situated within a
basaltic flow sequence of the central Handy Lake Volcan
ics (Trowell 1978). To date no economic mineralization
has been reported from these areas, but they warrant ex
ploration.
Sturgeon Lake Sub-Area
At Sturgeon Lake ultramafic intrusions with mafic highmagnesian tholeiitic gabbro differentiates occur north of
Post Lake and on Mountain Island (Trowell 1974d, 1976;
Zalnieriunas 1978). Nickel sulphide was reported in a dia
mond-drill hole from one of the bodies located north of
Post Lake (Assessment Files Research Office, Ontario
Geological Survey, Toronto). A band of pyroxenite cumu
late that forms a partial ring around the Bell Lake Alkaline
Complex contains no known mineralization but may war
rant investigation (Hoad 1970; Trowell in prep).
Differentiated multi-phase mafic intrusions, locally
with minor cumulate ultramafics, are situated within low
ermost mafic metavolcanic sequences west of Sturgeon
Lake (Trowell 1975, in prep). These bodies locally contain
abundant titaniferous magnetite.
Sioux Lookout Sub-Area
In the Sioux Lookout area, mafic and ultramafic intrusions
situated within the Southern Volcanic Belt may be good
exploration targets (Bartlett /nTrowell etal. 1978).
Wabigoon-Manttou Lakes and Kakagi-Atikwa Lakes SubAreas
The association of copper-nickel deposits with mafic and
ultramafic intrusive rocks has been well established by
previous exploration and mapping near Rowan and
Atikwa Lakes in the southwest (Davies 1973; Kaye 1973;
Assessment Files Research Office, Ontario Geological
Survey, Toronto), and near Nabish Lake, east of Eagle
Lake and at Contact Bay of Wabigoon Lake (Assessment
Files Research Office, Ontario Geological Survey, Toron
to).
Lesser amounts of copper and copper-nickel miner
alization have also been established in the large gabbroic-anorthositic intrusion.at Mulcahy Lake (Moorhouse
1941, Davies and Watowich 1958) west of Eagle Lake,
and in a number of small bodies either marginal to the
Atikwa Batholith (e.g. southwest of Wabigoon Lake), or in
ternally emplaced within the volcanic belts (e.g. Boyer
Lake in the Manitou-Stormy Lakes area) (Blackburn
1979a).
Interest in base metal association of this kind was
generated in the 1950s with the discovery of copper and
copper-nickel deposits near Atikwa and Populus Lakes.
This subsequently led to the development of the Kenbridge mine near Populus Lake, and the Maybrun mine at
Atikwa Lake (the latter being a copper-gold association
reportedly in mafic metavolcanics) (Davies 1973).
Blackburn (/nTrowell etal. 1978) has recently recog
nized that the Mulcahy Lake gabbroic intrusive body is
layered and bears some resemblance to other layered in
trusions that host important ore deposits. It therefore must
be considered as a potential host for copper-nickel min
eralization, or, by analogy with the Dor6 Lake Complex at
Chibougamau, Quebec, copper-gold mineralization (AlIard1976).
The majority of mafic-ultramafic intrusive bodies dis
cussed above are located at the edge of the Atikwa Ba
tholith. Many of the more dioritic phases can be consid
ered to be derived by hybridization of mafic volcanic
country rock by the emplacement of the batholith,
whereas the huge volume of the mafic-ultramafic bodies
suggests them to be primary igneous phases. Whatever
their origin, their spatial distribution at the margin of this
batholith is a good exploration guide.
To date little mineralization has been found associ
ated either with differentiated ultramafic to mafic sills at
Kakagi Lake, discussed by Davies and Morin (1976) and
Kaye (1974a,b), or mafic sills intruded into Katimiagamak
Volcanics (Kaye 1974a,b). However, Edwards (1978) has
drawn attention to copper occurrences in mafic-ultra
mafic sills near Pipestone Lake.
Blackburn (1979a) has suggested that anomalously
high nickel values in lake sediments found by Coker and
Nichol (1975) in the Manitou Lakes area indicate that the
basal part of the thick Wapageisi Volcanics mafic flow se
quence is a favourable target for sulphide mineralization.
Uranium and Other Lithophile Elements
In a recent discussion of the geology of the English River
Subprovince, Breaks etal. (1978) have given a compre
hensive discussion of both uranium mineralization and li
thium-caesium-beryllium-tantalum-tin-bearing
pegma
tites, that mostly pertains to the area north and west of
that under discussion here.
In their discussion of uranium, Breaks et al. (1978)
emphasize its occurrence in two distinct lithologic situa
tions: metasedimentary migmatite, and potassic granitoid
association. In addition to their comments it is to be borne
in mind that extensive metasedimentary migmatite lies
along the northern edge of the Savant Lake Crow Lake
belt, between Bluett Lake in the east and at least as far as
Dryberry Lake in the west. The project by Breaks et al.
(1978) terminated southward at 49045'N, so that the ura
nium mineralization potential southwest of Eagle Lake
was not studied by them. The same lithologies that host
uranium in Temple Township, south of the town of Vermi
lion Bay, appear to continue marginal to the Dryberry Ba
tholith, possibly continuously around this south-protrud
ing lobe of the English River Subprovince within the
Wabigoon Subprovince.
Breaks etal. (1978) in discussing lithophile elements
in highly fractionated residual diatexitic pegmatite phas
es, mention that ". . . in the Dryden area of Wabigoon
Subprovince several occurrences containing lithium, and
beryllium, and a single pollucite-spodumene showing lie
near the eastern end of a relatively extensive tourmalinebearing homogeneous to inhomogeneous muscovite dia
texite pluton situated between Vermilion Bay and Ghost
Lake." These are in Zealand and Brownridge Townships,
and in Webb Township immediately south of the Lateral
Lake stock.
23
SAVANT LAKE—CROW LAKE
Discussion of Mineralization,
and Exploration Guide-lines
We have attempted to illustrate how mineral deposits in
the area are associated with specific lithologies and are
situated at specific stratigraphic levels within the vol
cano-sedimentary belt. By comparison of mineralization
type, associated host rocks, and stratigraphic setting
with similar parameters of known mineralization in other
volcano-sedimentary belts we can outline the location of
other favourable lithologies and stratigraphic settings
within the present area.
Volcanogenic Base Metal Deposits
In Japan, Kuroko type (Sato 1977) base metal sulphide
deposits, similar in many respects to those at Sturgeon
Lake, are likewise associated with felsic pyroclastics and
redeposited fragmentals. They occur at a discrete strati
graphic level, formed over a duration of perhaps 0.3 to 1
million years and extend for 500 km along the volcanosedimentary belt within the island-arc environment (Ueno
1975). While direct application of the mechanism of plate
tectonics has not been substantiated for Archean time,
physical-chemical parameters as applied to magma gen
eration of comparable chemistry, and mode of deposition
are a basis for comparison. In this respect we can pro
pose that comparable lithologies to those at Sturgeon
Lake, as for example, the Northeast Arm Volcanics, the
lower Handy Lake Volcanics and the lower volcanic se
quences at Eagle and Wabigoon Lakes are possible tar
gets for base metal exploration. Samples collected from
these and other areas of similar lithology are presently
being radiometrically dated through a geochronological
program run in conjunction with this project (Davis et al.,
in prep.). These ages are intended to complement litho
logic correlations and aid in more precisely identifying
discrete stratigraphic levels favourable for massive sul
phide mineralization.
Volcanogenic Copper-Gold Deposits
Again, in comparison with mineralization types of Japan
and other island arc environments we should consider
the question of Besshi-type sulphide deposits. These pyrite-chalcopyrite-(gold) deposits are generally associ
ated with deep water, intermediate to mafic volcanic
rocks and associated chemical and clastic sedimentary
rocks (Mitchell and Bell 1973; Sawkins 1976). In the pres
ent area the Maybrun deposit (Davies 1973) may be of
this type. Other areas of comparable lithologies are the
lower Jutten Volcanics in the area of Armit and Never
freeze Lakes where interbedded quartz-magnetite iron
stone and chert, locally with graphitic and sulphidic (py
rite, pyrrhotite, trace chalcopyrite and sphalerite)
siltstone occur together with mafic volcanic amphibolite.
A comparable situation occurs at the North Pines Mines
24
Limited deposit near Sioux Lookout (Johnston 1972)
where trace chalcopyrite and sphalerite accompany the
dominant pyrite-pyrrhotite assemblage in a host of carbonatized mafic hyaloclastite.
Sawkins (1976) has emphasized that in addition to
occurring within mafic volcanic sequences, structural
complexity and proximity of thick sequences of wacke
are characteristic of Besshi-type deposits. The occur
rence of scattered Cu-Au deposits at the contact be
tween mafic metavolcanics of the Central Volcanic Belt
and sandstone of the Minnitaki Group northwest of Sandybeach Lake is suggestive of this type of environment.
All of the above-mentioned deposits occur along the
north side of the Savant Lake -Crow Lake Belt, and in
fairly close proximity to the more northerly of the two clas
tic zones discussed under "General Stratigraphic Rela
tionships".
Gold Deposits
In considering gold deposits in the area it is important to
note that gold mineralization in the Timmins or Porcupine
Camp of the Abitibi Belt appears to be intimately associ
ated with ultramafic (komatiitic) rocks, felsic porphyry
and carbonate horizons (Pyke 1975; Karvinen 1978).
Sea-floor alteration/metamorphism of the ultramafic flows
and specifically fragmentals has been postulated for ini
tially concentrating gold, allied with subsequent intrusion
of porphyries. Structure may be important in providing
channelways resulting in gold being deposited in specific
structural sites as economic-grade deposits.
In a previous discussion, Mackasey et al. (1974)
noted the close spatial relationship of many gold deposits
to mafic metavolcanics, and invoked felsic intrusions as
concentrating agents. In contrast to Timmins, ultramafic
flows are infrequently found in the present area. This fact
could, to some extent, explain the paucity of economic
deposits in contrast to numerous sub-economic occur
rences. The St. Anthony mine is somewhat similar to the
gold deposits of Timmins and Porcupine in that a por
phyry hydrothermal system has been superimposed on a
carbonatized mafic flow stratigraphy. As well, a carbo
nate-breccia unit (Trowell 1977; Gordanier 1975) com
posed of carbonatized, possibly ultramafic, hyaloclastite
carries anomalous gold in the 10-200 ppb range, with
higher values in cross-cutting quartz veins. Perhaps the
lack of a superimposed hydrothermal system precludes
the development of an ore-grade deposit. However, so lit
tle of the unit is exposed, further investigation is war
ranted. A carbonatized mafic unit is similarly found in the
Goldrock camp (Blackburn 1979a), stratigraphically be
neath the felsitic units that host gold mineralization. How
ever, no porphyry body occurs close by, though the pos
sibility of such a body at depth is not ruled out. Ultramafic
intrusions and rare flows with apparent komatiitic chemis
try occur at Armit Lake. They show a close spatial rela
tionship to quartz-magnetite ironstone units, both being
likely favourable areas for gold mineralization.
Copper-Molybdenum Deposits
Porphyry copper and molybdenum deposits in the area
appear to be of two types. One type, such as in the Beidelman Bay Pluton, is analagous to island-arc porphyry
deposits described by Lowell and Guilbert (1974). The
Lateral Lake Stock (Colvine and Mccarter 1977; Page
1979) is representative of the second type, comparable
to those that occur in continental margin magmatic belts
developed within continental crust (Hollister 1975). It is of
interest that lithophile element mineralization such as tin
and tungsten occurs in a similar continental setting
(Pearce and Gale 1977) similar to the tungsten-tin occur
rences situated at the same stratigraphic level as the Lat
eral Lake molybdenum mineralization.
Copper-Gold in Intrusive Rocks
At Chibougamau in Quebec, copper-gold mineralization
is associated with shears in the anorthosite zone of the
Dore Lake Complex marginal to the later, felsic Chiboug
amau Pluton (Allard 1976). The Mulcahy Lake Intrusion
(Blackburn /nTrowell et al. 1978) is a similar differentiated
body, but lacking an analogue of the anorthosite zone. Al
lard (1976) considers the Chibougamau ores to be epi
genetic, but whether they are epigenetic or syngenetic,
the analogy with Mulcahy means that a search for cop
per-gold mineralization marginal to late felsic phases
may be worthy of investigation.
Platinum and Platinoid Group Elements
At the current high price of platinum and platinoid group
elements, a systematic study of all the ultramafic bodies,
especially those that show magmatic differentiation al
lowing cumulate crystallization and the concentration of
particular phases at specific stratigraphic heights within
the intrusions (e.g. Mulcahy Lake Intrusion) should be
considered.
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SAVANT LAKE—CROW LAKE
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26
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1975: Metallogenic Relations at Sturgeon Lake; Proceedings
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1975: Geochemistry of a Carbonate Breccia Unit in N.W. Ontar
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1977: Geological and Geochemical Survey of Lyon Lake and
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1977: Geological Setting of Volcanogenic Massive Sulphide De
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1975: An Appraisal of the Nature and Source of Porphyry Cop
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1973: Wall Rock Alteration and Trace Element Geochemistry of
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27
SAVANT LAKE—CROW LAKE
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1976: Geochemical Dispersion in Wallrocks of Archean Massive
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1941: Geology of the Eagle Lake Area; Ontario Department of
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1974: The Geochemistry of the Lyon Lake-Claw Lake Sulphide
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1974: Ontario Mineral Map; Ontario Division of Mines, Map 2310,
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Chart A
Savant Lake-Crow Lake
Metavolcanic-Metasedimentary Belt
90C
30'
SYMBOLS
LEGEND
Geological boundary
Alkalic Intrusive Rocks
Syenite
Anticline, syncline, with plunge
Felsic Intrusive Rocks
Fault
Stratigraphic top; pillow and
sedimentary structures
Mafic and Ultramafic Intrusive Rocks
Scale 1 6,336,000 or 1 inch to 100 miles
Metavolcanics
Intermediate and felsic metavolcanics
Mafic metavolcanics
500 r
CHART A
PRELIMINARY STRATIGRAPHIC UNITS
AND STRUCTURAL GEOLOGY
SAVANT LAKE - CROW LAKE
METAVOLCANIC - METASEDIMENTARY BELT
Districts of Kenora, Rainy River, and Thunder Bay
Scale
1 : 506,880
8
Kilometres 10
49'
30
93
30
10
20
32
24
16
30
40
50
Miles
Kilometres