-
- 85 -
la Ronge-Wollaston Belts Base Metals Project: Geo!]e Hills,
Johnson and Kaz Lakes
and Geikie River Areas by W. Coombe
In 1977 an examination of several zinc-lead, lead and copper
occurrences,
hosted by Aphebian Wollaston Group metasediments of the
Wollaston domain, was under-
taken. Recent advances in the understanding of sandstone-type
zinc-lead deposits
prompted the writer to focus on two widely separated and
contrasting areas of mine-
ralization. In the Sito Lake area (Fig. 1) there are at least 5
known zinc-lead
occurrences within an area of 200 km2 . The mineralization is
restricted to a
quartzite membeY of the lower part of the Wollaston Group of
pelitic and semioelitic
gneisses (see Potter, this volume).
The George Lake area, approximately 80 km2 (where Falconbridge
Nickel Mines
Ltd. have outlined an uneconomic deposit of zinc-lead of 5
million tons averaging
2.65 percent Zn and 0.35 percent Pb (Karup-M¢11er and Brummer ,
1970)) was mapped at
a scale of 1:12,000 by the author, utilizing previously cut
grids. The mineralized
zone occurs near the top of a thick grey quartzite unit, in the
lower part(?) of
the stratigraphic sequence.
In addition to these areas, the author visited the following (Fi
g . 1) :
(a) Hills Lake (zi~c-lead)
(b) Johnston Lake (Marina showing) (lead)
(c) Kaz Lake (copper)
(d) Geikie River area (copper-molybdenum in boulders)
George Lake Area
The rocks of the George Lake area belong to the Compulsion River
Fold Belt of
Pyke and Partridge (1967), Karup-M0ller (1970), Karup-M0ller and
Brummer (1970) and
the Courtenay Lake-Cairns Lake Fold Belt of Scott (1970).
The area mapped by the author (Fig. 2) extends from Courtenay
Lake in the south-
west, to George Lake in the northeast and is largely covered by
muskeg. Outcrops
are restricted in general, t o areas adjacent to rneltwater
channels e.g. George Lake
and Causier Lake channels.
Predominant meta-sediments, with minor intrusives and
?volcaniclastics occupy
a synform trending 055-060° (Assuming no other repetition of
strata they fo rm a
single synform). An estimated thickness of the sequence (Fig. 3)
in the southeastern
limb of the synform at George Lake i s 5000 m. The geology of
the northwestern l imb
-
D . D E] . .
- 86 -
A rho b c:i1co Fo, rnor,on
IH•h• •onl
Wollo1ton G roup Sup roc r uuo l Roe lu
IAohob,on)
104'
O 20 •o,m 0 20M,
Explanat ion
• O uon z11e -hos te d t •l"I C -leod occvrren ce~ 1 G• o•ge Lo
~• 2 Hil u Lo._ , ) Joh"ISOl'I lClitt 4 S,•o lWi 5 5,•o :; ; · 6
5·•o :sw1 7 G eo rge a Foole Lo._• 9 Segm,erH Lot\•
+ MePo ·coni;, l cm• r c:ne o nd m e1 0 - a rll.ose ~h o sre d
coop•, occur, e nc• 1
l ll:ofu1• t o\:e 2 Ko z: Lai.• J. J cu ,1 c e l..o k • 4 J u
>\ o La••
• Robb,r La ite uron, 1,1m m ine
& Kitr Loh· uron1um dei;:0,11
• Dudd,,d ,ge Lake, meto .. cong l ome, o re Ol"ld quorr1
:1e-hosted u,o n ivm 1- cooDt r) occ.v r r e nce X Mud l o kP
molybd e n1.1m occurte ric e
Bo,emenl Granite !Remobil,zed A rch eon '?) 0
Fig. 1 . Location map, s howing distribution of selected mineral
deposi t t ypes within the Wollaston domain. Areas investigated
during the s tudy: I, Sito Lake area; II, George Lake area; III, Hi
l ls Lake; IV, Johnson Lake; V, Kaz Lake; VI, Geikie River
area.
is l ess c l early understood . due to lack of outcrop
(concentrated i n the Causier Lake
a rea) and control (no cut lines) . Estimated thickness i s in
exc ess of 1000 m.
The Southeastern Limb . On the southeastern l imb 'way-up'
structures i ndicate (i) a
general f i ning of lithotypes towards the northwest and (ii) a
change i n charac ter
from terrestrial / shallow marine t o calcareous marine
sedimentation.
Lower Me t a - a rkose Unit . The Lower Meta-arkose unit is
exposed at the end of
Courtenay Lake and can be traced intermittent ly northeastwards
. It appears to
thicken i n tha t direc tion , ranging from approxima tely 1000
min the s outhwest
to 2000 min the northeast.
-
• A,p-py-po-eo-• occ1,,11,.,,o
0
0
- 87 -
Nott "'••ttern ,...,.,
)ohnson Riv., b•rtlotith (.,. .. .....i ........... ,
J km
2 Mi
LEGEND
~ . . 6J ~ EITJ [] j."';"1 t.:..:..J
10J'A5'
SI••• ""'ut
G,.,. ouanci•• unit
Fig . 2. Geological sketch map of geology of the George Lake
area.
The unit comprises a elastic member and an extrusive (?intrusive
in part)
member. The elastic member which predominates , includes a
variety of lithofacies,
ranging from cross-bedded me ta-arkoses, through graded s
cour-and-fill units to
boulder meta-conglomerates and breccia-meta-conglomerates. All
are characterized
by a pink-cream (to pink-red) colour and an abundance of
accessory magnetite and
ilmenite. Cross bedded units are commonl y less than 15 cm in
thickness, and
indicate tops to the northwest. Boulder meta-conglomerates are
usually less
than 2-3 m thick and composed of slightly flattened clascs up to
30 cm in length
(average length: width ratio~ 3:1) . Boulder: matrix ratios are
commonly high
-
s.w.
. . . . . . . ..
.,/ .,/
..,.,,, ...---
----- -- --
...........
- 88 -
N.E.
... .. . .
UPPER META- ARKOSE UNIT
CALCAREOUS QUARTZITE UNIT
Asp, PY, po, go, sp
CALCAREOUS META-ARGILLITE UNIT
~ PY, PO SLATE UNIT
- PY, po ~ Sp, ga, py, po
. . . . . . . e.O."'c, o·.~c,·•o
-
- 89 -
(3: 1). Meta-conglomerates are poorly sorted and polymictic;
predominant clasts
are of whitish-grey feldspathic quartzite with lesser vein
quartz and granite
cobbles . Pebbly lenses in the troughs of c ross-beds are
coonnonly composed of
quartz and (K-) ~eldspar clasts less than l cm in diameter.
Amphibolite occurs at least at two horizons within the Lower
Meta-arkose
unit. The lower amphibolite is fairly heterogeneous and
comprises predominant
amphibolite with epidosite lenses and sheets and intercalated
semipelite and
pelitic gneisses . Some amphibolite layers resemble
hyaloclastite, but no obvious
pillows were observed. The upper amphibolite is more
homogeneous, lacking marked
pelit ic interlayers, and ranging from a massive amphibolite to
amygdaloidal and
podifo rm t ypes. These two amphibolite units can be traced
continuously across
the area by their high-relief magnetic expression.
The southeastern contact of the Lower Meta-arkose unit is
grarlational over
a width of up to 1000 m with Biotite (after amphibole) granite.
Towards the contact
the meta- arkoses become less distinctly cross-bedded, and relic
bedding is evi-
denced only by thin lenses of oxides . The field relations
suggest that the
granite is intrusive , although the contact is in part, sheared.
Shear zones,
up t o 100 min width, transect t he basal beds and trend
055-060°, approximately
parallel t o t he bedding. Where the s hear zone cuts the
porphyroblastic facie s,
the meta-arkose becomes an augen gneiss, with quartz-sericite
matrix.
The uppermos t 600 m of the Lower Meta-arkose unit appears to be
only present
towards the nor t heast, and is we ll exposed at the southern
end of Souter Lake
where it comprises massive and subordinate thin-bedded (less
than SO cm) pink
(to maroon) ' glassy' quartzites and feldspathic quartzites. A
distinctive
quartz- sericite s chist , with porphyroblasts of andalusite and
biotite after
staurolite (Scott, 1970), i s f ound approximately 240 m below
the top of the
unit. Likewise, layers of meta-argillite and grey quartzi te
also occur. They
are up to 1 m but an average 10 to 20 cm in thickness and form
beds less than
15 m thick.
Grev Quartzite Unit . The Grey Quartzite unit i s distinguished
by not only the
absence of pink meta-ar koses but, apart from minor amounts
within gr ey biotitic
quartzites of the uppermost Lower Meta-arkose unit , coi ncides
also wi th the
appearance of sul phides in the sequence. It thins from appr
oximately 1000 min
the vicinity of George Lake to less than 350 ma t the north end
of Court enay
Lake.
The basal bed is a black slatey meta-ar gillite, approximatel y
80 m thick,
-
- 90 -
that contains abundant porphyroblasts of chiastolite at i t s
base, and becomes
graphitic and pyrite-pyrrhotite bearing, towards the top. Ahove
this bed the
unit is mostly composed of a variety of grey to grey-white, and
rarely white
feldspathic quartzites and quartzites with intercalated
meta-argillites. The
unit is characterized by rapid facies changes both along strike
and across it .
Immediately overlying the black slar.ey meta-argillite are
approximately 150- 200 m
of thin-bedded grey, pyrrhotite-bearing, biotite quartzites and
interlayered meta-
argillites. These quartzites commonly show graded bedding and
scour-and-fill
structures. The overlying 350 mis unexposed; frost - heaved
boulders contain a
number of pebble and boulder meta-conglomerate layers. Clasts of
quartz and
feldspar predominate with lesser meta-argillite and pebbly
quartzite . The quart-
zite clasts are up to 15 cm in length.
The uppermost 500 m (at George Lake) is comprised of an
interlayering of
several quartzite types which range from graded, gritty units a
few centimetres
thick, to garnetiferous biotitic varieties that show lensing
from 1.5 m t o less
than 10 cm. Meta-argillites (generally l e ss than 25-30 cm
thick) are common
within this part of the sequence both as graded tops and
discrete thinly layered
beds. Quartzites with beds less than 1 cm in thickness are also
present.
The ore zone is unexposed, but frost-heaved boulders from this
zone differ
from the rest of the unit in that they are more massive and
finer textured.
They vary from a grey to grey-white to whi te feldspathic
quartzite. The follow-
ing description of the zcne is extracted from Karup-M~ller and
Brummer (1970) :
1, The mineralized zone occurs approximately 25-30 m below the
top of the
Grey Quartzite unit.
2. The zone averages 30-40 min width, and extends for
approximately 600- 700 m
along strike.
3. Mineralization is concentrated in a grey quartzite, and
appears to decrease
with increasing biotite content.
4. The grey quartzite contains up to 15 percent feldspar, minor
biotit e,
muscovite and rare garnet. The grey quartzite becomes a white
quartzite wi t h
decreasing feldspar, biotite, muscovite and garnet. The biotite
quartzit e
contains variable amounts of biotite, garnet, muscovite, rare
tremolite and
hornblende.
5. Sphalerite is the predominant sulphide, minor galena and pyri
te are oft en
present. Pyrrhotite is erratically distributed.
6. The sulphides occur as disseminated specks, averaging 1 mm in
diameter,
and rarely as hair-line cross-cutting fracture fillings.
-
- 91 -
7. The mineralized zone has been traced south-westerly at least
2.5 km.
Slate Unit. The Slate unit overlies the Grey Quartzite unit and
at George
Lake is approximately 500 m thick thinning to half this
thickness at Courtenay
Lake. The lowermost member is a grey meta-argillite,
approximately 25 m thick,
that overlies biotite (-garnet) quartzite of the Grey Quartzite
unit. The Slate
unit is composed of a number of lithofacies, but slates and
slatey argillites
predominate. These are very fine-grained, dark-grey to black,
thin bedded in
part, and varyingly graphitic. They co!Dlllonly contain up to 1
to 2 percent
pyrite, both as disseminated blebs (framboids) and later
fracture-fills. In
detail they vary from dark siltstone to mudstone. The slates
occur as two
distinct bands, reflected by high magnetic relief which average
80-100 min
thickness and are occasionally garnetiferous. Distinctive chert
bands, cherty
quartzites, greywacke (tuff), and minor laminated meta-argillite
occur as inter-
beds. The chert is well bedded, striped, and up to 20-30 m
thick. Individual
beds average 1-2 cm in thickness, and alternate light and dark
grey. The
cherty quartzites are more thickly bedded, cream-buff, and very
fine-grained.
Up to 1 percent pyrrhotite is the predominant sulphide in the
cherts and cherty
quartzites, occurring as disseminations. Although thin the chert
beds appear
continuous over at lease 4 km.
Calcareous Meta-argillite Unit. The Calcareous Meta-argillite
unit is approxi-
mately 800 m thick at George Lake, and thins slightly to the
southwest. It
comprises predominant meta-argillaceous laminites with
calcareous layers, and is
typically light to medium grey, delicately laminated (1-2 llllll
scale) and siliceous.
The calcareous component may range from less than 5 percent to
consistent calc-
silicate and marble bands. A distinctive unit along the
northwestern shore of
George Lake is a very fine-grained well laminated (1-5 llllll)
greenish rock,
composed of alternating green calcite-tremolite and quartzose
meta-argillite
with some thin layers of white, calcareous, feldspathic
quartzite. Elsewhere,
light brown layers, less than l m thick, of
quartz-feldspar-garnet-tremolite
(scapolite) occur. Highly calcareous light grey layers, 1-2 m
thick, are
occasionally present, especially near the top of the unit in the
southwest.
Dark grey and black meta-argillites and slatey meta-argillite~
are present
as layers within the Calcareous Meta-argillite unit. Northeast
of Courtenay
Lake, dark grey and black meta-argillites and slatey
meta-argillites are inter-
layered with cherts and cherty quartzites that resemble those in
the Slate unit .
They present high-relief magnetic signatures, which enable the
horizon to be
traced intermittently to the northeast. Near George Lake the
cherts and cherty
-
- 92 -
quartzites appear to be absent.
A meta-argillite bed near George Lake, exposed along the
northwest shore
of the small lake, 1000 m northwest of Souter Lake contains
abundant arseno-
pyrite. The arsenopyrite is present as fine disseminations
(earlier) and
coarsely-recrystallized porphyroblasts (later). In places it
comprises up to
50 percent of the rock over a few centimetres, but probably
averages less than
5 percent. It is associated with abundant pyrite, pyrrhotite and
minor galena
and sphalerite. Arsenopyrite-bearing quartz veins anastomize
throughout the
bed, and there does appear to be a marked concentration towards
the veins.
The same association is also seen 5.8 km along strike to the
northeast,
where the zone appears to be continuous along strike for 120-150
m. At this
locality fracture-fill relationships were observed by the
author. Grab samples
* from this zone, taken by E.F. Partridge ran up to 8 percent Pb
.
Calcareous Quartzite Unit. The Calcareous Quartzite unit appears
to be restric-
ted to the northeast part of the area, and possibly thickens
northeasterly into
the Spence Lake region. It is approximately 350 m thick
northwest of George
Lake, and thins out about 2.4 km to the southwest where it may
be truncated by
the Upper Meta-arkos e unit. Though heterogeneous, the unit i s
characterized by
white calcareous, massively bedded feldspathic quartzites, up to
several meters
thick, interlayered with laminated siliceous argillite,
calc-silicate and impure
marble. Northeast of the area are distinctive brown-weathering
intraformational
carbonate breccias and near Spence Lake apparent dessication
cracks were obser-
ved. In general these occur in beds less than 50 cm to several
meters thick.
Upper Meta-arkose Unit. The Upper Meta-arkose unit appears to be
at least 600 m
thick, and comprises predominant pink and pink-grey
medium-grained meta-arkoses.
These are commonly massive, but occasionally show light grey and
pink colour
banding on a scale of 1-2 cm.
The basal beds, especially to the southwest, are formed by
distinctly banded
calcareous meta-arkose, up to 50 m thick. Alternating 1-2 cm
thick layers are
rich in actinolite and epidote and contain traces of
calcite.
The Northwestern Limb. On the northwestern limb of the synform
outcrops ar e confined
to an area southwest of Caus ier Lake. The creek flowing
southwesterly f rom Causier
Lake follows the contac t between two subtly different pelitic
units.
Northwest of the creek, the 'northwescern pt lites' ar e t
ypically mottled red-brown
* DMR Assessment fil e 64E12SE0021
-
- 93 -
and dark-grey weathering, phyllitic to. schistose rocks which
include variable amounts
of garnet and sillimanite and ubiquitous biotite and muscovite.
They are generally
massive, although some thin (up to 15 cm) more psammitic
(silty?) bands occur.
White, tremolitic quartzite that forms a massive bed
approximately 30-50 m thick is
exposed along the creek. To the northwest it becomes
interlayered with the pelites.
White, muscovite-bearing pegmatite invades the pelites, as
sheets up to 10-15 m thick
sub-parallel to the layering/foliation. Thes~ sheets are
commonly sheared and
granulated.
The heterogeneous 'southeastern pelites', which differ from the
northwestern pelites by containing little garnet and sillima.nite,
by being gritty in character and
by being interlayered with cherts, cherty-quartzites and
calc-silicates, outcrop south-
east of the creek. For approximately 300 m southeast from the
creek, the predominantly
biotite-muscovite pelites, contain a variable proportion of
grit-sized clasts (quartz
and felsic fragments?). In some thin units very angular clasts
(?meta-arkose) reach
dimensions of more than l cm. Layering is present locally in
these rocks and the
entire sequence may represent a greywacke-turbidite succession.
Southeast of the
gritty pelites, the rocks are also characteristically pelitic,
with thin psammitic
bands, but here dark green-black amphibole may form up to 20
percent of the rock.
These are thought to represent the equivalent of the Calcareous
Meta-argillite unit
farther southeast.
Pyrite and pyrrhotite are disseminated in trace amounts
throughout, but are more
abundant in the more siliceous layers.
Structure and Metamorphism. Bedding is well preserved throughout
t he area, and primary
sedimentary structures and textures can be readily
identified.
In addition to bedding (s0
) two ages of foliation (S1
and s2) are cot!lllonly developed. s
1 is parallel to s
0, and trends 050-060°, except in two isolated loca-
lities where it is axial planar to tight, shallow, southwesterly
plunging F1
folds.
The F1
folds were found near the south end of Causier Lake (within the
northwestern
pelites) and northwest of George Lake (within the Calcareous
Meta-argillite unit).
They possess subvertical axial planes, and are presumably s
ynchronous with the major
synform of the area. Locally a rodding lineation (L1) i s
parallel to F1fold axes.
s2 , a strain-slip cleavage, is present throughout the area, in
the cores of minor Z-style F2 folds. The F2
structures plunge steeply northeast and have sub-vertical
axial surfaces trending 035-0li0°.
No significant faults were identified. Numerous narrow shears,
parallel to s1,
-
- 94 -
are present throughout the area. These are expecially prominent
towards the base of
the Lower Meta-a rkose unit , and within pegmatites that invade
the northwestern pelites
of the Causier Lake area ,
Metamorphic conditions appear to range from the upper
greenschist to the uppe r
amphibolite facies. Generally there appears to be an increase in
grade towards the
southeastern and northwestern margins of the area.
Indicator minerals include muscovite, garnet,
tremolite-actinolite, andalusite,
staurolite, 'hornblende ' , and sillimanite.
l. Along the southeastern margin, dark green-black amphibole is
predominant within
the amphiboli te horizons. Rare pelitic interlayers are
coarse-grained and gneissic.
2. Within the upper part of the Lower Meta-arkose unit,
chiastolite, andalusite and
s taurolite have developed as porphyroblasts within iron and
alumina rich pelitic
interlayers.
3. Garnet is widespread through the area.
4. Tremolite-actinolite is the predominant amphibole within
calc-silicate horizons
of the Calcareous Me ta-argillite unit.
5. Muscovite is sparingly present within rocks of the
southeastern limb, but
abl.l;ldant in pelites of the northwestern limb.
6. Sillimanite is c ommon within the 'northwestern pelites' of
the Causier Lake area
The mai n me tamorphic event appears to have been approximately
synchronous with
F1
. Rotation of sillimanite knots occurred duri ng F2
.
The Bills Lake Zinc-Lead Occurrence
The Hi lls Lake Zn-Pb occurrence (Fig. 4) lies within the Morell
Lake (W ~) area.
The geology of the area has been described by Chadwick (1966).
In the vicinity of
Hills Lake there are two major rock units . Granitic rocks,
which are part of the
northwestern flank of the J ohnson River ba tholi th, occupy
much of the area. Itmne-
diately in contact with the gr ani tic r ocks (and pres umably
unconformable upon them)
a t Hills Lake i s a s eries of pelitic and semipe litic
gneisses containing some impure
quartzite layers. The pelites a r e c ommonly gr aphit i c , and
often garnetiferous. Over -
lying (?) these gneisses is a seq uence of meta- arkosic and
calc-silicate rocks.
Numerous mineralized boulders have been discovered, over an a r
ea of approximately
SOOm x 200 m, at the south end of the Hills Lake. These average
l ess than one meter
i n maximum dimension and are sub-angular. They are predomi
nantly medium- to coarse-
grained ' quart zit e ' and vary from light grey (least
mineralized) to dark buff -brown
(highl y mineralized). The 'quartzite ' contains a high percent
age of fel dspar (40-50
-
57°34'
- 95 -
103· 55'
103°55'
~ Wolloston G roup met ased iments f+"""J G ran itic rocks -
largely 'Johnston L±_J Ri ver Bat hot i th' ( assumed basement)
® Mineral ized boulders
/ Em conductor
Fig. 4 . Location of Hills Lake Zn- Pb occurrence. Geo l ogy
after Chadwi"ck (1966)
percent) and va=ies from an equigr anular, sugary- t extured
rock to a ' br eccia' . The
' breccia ' is composed of large angular feldspars ( ?porphyrobl
asts) , 3-4 mm in diameter ,
and quartz grains set in a finer quarrzo- feldspathic matrix. It
is uncertain whether
t his ' breccia ' is of depositional, me tamorphic o r tectonic
origin.
Mineralization consists of sphalerite and mi nor galena in
association wi th
pyrite, pyrrhoti t e a nd magneti t e . Spha l erite (_dark
black variet y) and magnetit e are
predominant . The sul phi des occur as f ine and coarse di
sseminations throughout boc.h
-
- 96 -
the equigranular quartzite and 'breccia'. In addition slip
planes coated with
pyrite, sphalerite and magnetite are abundant, both concordant
and discordant to the
weak foliation.
A diamond drill hole near the southern end of Hills Lake
intersected 3 percent
* Zn over a core length of 3.6 m. The host rock is described as
'feldspar-biotite-hornblende rock with indistinct banding'.
The Marina Lead-Zinc Occurrence, Johnson Lake
The Marina occurrence is located on the northwestern shore of
Johnson Lake
(Fig. 5), on the northwestern flank of the Johnson River
Batholith (Scott, 1969), an
assumed Archean basement inlier (Money et al., 1970), the
margins of which suffered
mobilization during the Hudsonian. Samples of granite from the
Marina occurrence
and adjacent area yield a Rb/Sr whole rock isochron indicating
an age of 1717 ± 68
m.y. i.e. late Hudsonian (Cumming and Scott, 1976).
Briefly the Johnson River Batholith comprises gneissic granite,
whereas the
overlying Wollaston Group metasediments are formed predominantly
by pelitic and meta-
arkosic rocks with local calc-silicates (Scott, 1969).
The Marina showing oc~rs in a 'quartzite' in direct contact with
the catacla-
sised augen granite. At the contact with the mineralized
'quartzite', the granite
is cream-pink weathe~ing whereas elsewhere it is pink-red
weathering. The contact
itself is exposed in two outcrops and is somewhat obscure. In
one outcrop there is
little evidence of a chilled margin, and the contact is marked
by an increased amount
of pegmatite, which locally encloses 'xenoliths' of semipelite,
whereas in the other
it is marked by a narrow (10 cm) zone of chilled granite with
abundant quartz strin-
gers, and in places a biotite-rich selvage. A pod of
near-massive fluorite occurs
at the contact, together with abundant amazonite-bearing
pegmatite.
The 'quartzite' bed varies in width from approximately 3 m to 15
m, this varia-
tion possibly being in part original, but probably being largely
due to cross-cutting
by the granite. The 'quartzite' itself is white weathering,
coarse-grained and
comprises approximately 70 percent quartz, 25-30 percent
feldspar and 1-2 percent
biotite. It is partly stratified, due to alteration of coarser-
(pebbly?) and finer-
grained beds. The quartz grains are commonly flattened in a
direction sub-parallel
to the cataclastic fabric in the granite. Minerali zation
consists largely of medium-
to fine-grained disseminated pyrite or marcasite, galena and
sphalerite. Galena pre-
dominates and is found as disseminations, as concentrations in
thin layers (? parallel
* DMR Assessment File 64El20020
-
57• 25'
- 97 -
+
+
~ Wollaston Group
{+ + +1 Granite , includes _.,-.- Em conductor
104• 10'
+ +
+ +
+ + + +
+ + + +
+ + +
+
+ + + + + + + +
O I 2 km ..., ______ _
O Mi .
104• 10'
metaseciiments
57• 25'
Johnson River Batholith
e Areas of mineralized quartzite bo~ders Fig. S Location o(
Johnson Lake Pb-Zn occurrence. Geo l ogy after Scott ( 1969)
to bedding) and as segregations filling discordant thin
fractures . Pyri t e/marcasite
commonly coats small vugs within the ho s t rock .
The mineralized quartzite is invaded by numerous sheets of
amazonite-bearing white
pegmatite . It is in sharp contact to the northwest with a dark
semipelitic to peli tic
biotite gneiss, which elsewhere near t he contact carries trace
to 2 percent of gra-
phite and abundant garnet. These graphitic pel ites form a
strong e l ectro- magnetic
conduc t or which has enabled the contact zone to be traced to
the southwest (Fig . 5.)
-
- 98 -
The Kaz Copper Occurrence
The Kaz occurrence (Fig. 6) is one of a number of similar copper
prospects in
an area of approximately 25 km2 The rocks belong to three units
(Scott, 1973) . In
the northwest are cordierite-sillimanite gneisses, which
possibly represent the base
of the Wollaston Group in the area. Above these are
meta-arkoses, which actually
show all gradations from meta-arkoses t o calcareous
meta-arkoses to biotite-actino-
lite rocks, calc-silicates and marbles, and arkosic
'meta-conglomerates', which are
the host rocks to the mineralization at Kaz.
Many variants of the 'meta-conglomerates• exist, some of which
are clearly con-
glomeratic in aspect whereas others are better described as
'nodular'. True meta-
conglomerates are t ypically 'candy-striped' and composed of
flattened white, fine-
grained arkosic(?) cla~ts in a pink arkosic matrix. Occasionally
the clasts are
somewhat more angular, and the rock approaches a breccia. The
'nodular' rock is
essentially a pink-cream to pink weathering meta-arkose with
white 'nodules' of
coarse-grained feldspar-quartz-amphibole. These nodules are
generally round, but
exhibit a range of shapes. They average 6-10 cm in diameter.
Their origin is not
clear ; they possibly represent clasts or concretions, however,
they do appear to be
different from irregular pods of pink-red pegmatitic neosome
that are also locally
present. In the mineralized zones the 'meta-conglo•erates' are
invaded by narrow,
straight-walled, pegmatites.
The mineralization is disseminated and consists of vis i ble
chalcocite, native
copper, "azurite" and "malachite". Covellite and bornite occur
in trace amounts. The
available assay data indicate mineralized zones, 1 m thick, that
lie parallel to the
bedding. These zones contain 1-2 percent Cu. Chalcocite and
native copper also occur
within pegmatite at Kaz Lake and elsewhere in the area
chalcopyrite and bornite bearing
pegmatites are reported (Rath and Morton, 1969; Scott, 1973).
Presumably these
represent remobilized copper segregations .
At Kaz Lake, numerous mineralized angular boulders have been
located. These
boulders are of pink and grey, equig ranular meta-arkose. Scott
(1973) notes that
these boulders contain chalcopyrite-galena, chalcocite-bornite
and chalcoci te-
chalcopyrite, There appear to be two basic types: (i ) pink
meta-arkose with dissemi-
nated chalcopyrite-galena (- s phalerite) and minor magnetite
and (ii) grey meta-
arkose with disseminated pyrite-galena (-spha lerite) and mi nor
magneti t e . None of these
mineralizations has been located i n outcrop.
-
56° 55'
56° .52'
- 99 -
0 I
104" 55 '
+ Cu - c. c . in 'meta - conglomerate' and meto - arkose
• Cu - c.c . in boulders of obove
o Ga - c . c . boulders
G Ga - c.p. boulders
2 km
I Mi .
[EZJ Predominantly meta - orkose , minor ca lc - silicate fifto]
Metoconglomerote ~ Pelitic gneisses (? basal Wolloston Group }
Fi g. 6 . Location of ~halcocite-native copper occurrence~ in
the Kaz Lake are3. Geology after Scott ( 19 73 ) .
-
- 100 -
Comparisons with Other Copper Occurrences in the Area. Similar
chalcocite-native
copper mineralization occurs at Janice Lake and Rafuse Lake in
'meta-conglomerate'
and at Juno Lake chalcocite-native copper-chalcopyrite
mineralization is present in
a possible outcrop of pink meta-arkose.
In addition to the 'in-place' mineralizations, a variety of
mineralized boulders
have been located. At Juno Lake, meta-arkose contains covellite,
chalcocite, bornite,
malachite, ilmenite, hematite and spinel. At Rafuse Lake, as
well as 'meta-conglome-
rate' containing chalcocite-native copper mineralization, two
boulders of a mafic-
ri ch 'biotite granulite', containing
galena-chalcocite-malachite-azurite-pyrite are
present (Scott, 1973).
The writer suggests that these mineralizations may all have
their source within
the same 'meta-conglomerate'-meta-arkose sequen~e. Furthermore
there seems a dis-
tinct possibility that the mineralization is stratiform, if not
essentially strata-
bound, and that the variation of assemblage is a product of
local zoning, as exempli-
fied below:
'meta-conglomerate'
chalcocite
native copper
(covellite)
(bornite)
(chalcopyrite)
pink meta-arkose
(chalcocite)
(native copper)
chalcopyrite
galena
(sphalerite)
magnetite
grey meta-arkose
(chalcocite)
galena
pyrite
increasing Fe/Cu ratio
Geikie River Copper-Molybdenum Occurrences
•
During 1967 E.F. Partridge prospected the Geikie River area
(Fig. 1) and dis-
covered a l arge number of mineralized boulders over a down-ice
trend of SO km and a
width of approximately 5 km. Detailed prospecting carried out
the fo llowing year in
two areas within the trend, s ub sequentl y led to the discovery
of molybdenum mi nera-
liza t ion at Mud Lake . Partridge logged the majority of
mineralized boulders as
" quartzite " and "feldspathic quartzite". These carry a trace
to minor amounts of
one or more of the following: disseminated pyrite , pyrrhoti te,
chalcopyrit e and
mol ybdenit e .
In 1977 the more accessible part of the mineralized boulder
trend, approximately
5 km s outh of t he Geikie River was visit ed. Outcrop i s spar
se and no minera lization
-
- 101 -
has been found in situ. The area is underlain by biotite
gneisses and rneta-arkoses
(Chadwick, 1968) and the writer observed outcrops of graphitic
pelitic gneisses
(?lower Wollaston Group) in the vicinity of the boulders. The
mineralized boulders
themselves are generally angular-subangular, uniform light grey,
massive, medium-
grained equigranular meta-arkos e with occasional
coarser-grained zones, which possibly
repres ent anatectic fractions. Mineralization is remarkably
uniform in a large num-
ber of boulders, and comprises disseminated chalcopyrite, with
minor pyrite, molybde-
nite and bornite(?). Chalcopyrite is very evenly distributed and
forms up to 1-2
* percent of the rock. Typical assay values returned 0.5-1
percen t Cu. Predominantly , the sulphides are intergranular,
average 0.5 DDll diameter, but tend to show some
segregation into anatec.tic fractions.
Some Aspects of the Mineralization and Metallogeny of the
Wollaston Domain
Base metal mineralization is widespread throughout the Wollaston
domain (Fig . 1)
and is, in large part, stratiform in nature. Available evidence
suggests that much
of the mineralization is essentially 'syngenetic ' with local
modifications due to
Hudsonian events.
Ray (1974, 1975) , Gilboy (1975) and Potter (this volume) have
recognized a cohe-
rent stratigraphy in the central part of the Wolla s ton domain.
The Wollaston Group
supracrustals lie unconformably upon Archean granitic basement
and comprise basal
pelites and semipelites (often graphitic) with subordinate
quartzites, overlain by
meta-arkoses and calcareous meta -arkoses and interlayered
calc-silicates . To a large
extent mineralization reflects the stratigraphy and is
particularly concentrated in
the basal sequence:
(a) In the graphitic pelites pyrite-pyrrhotite-graphite zones
occur, often in c lose
proximity to basement. The graphitic pelites are commonly
invaded by anatectic
pegmatites that carry miner values of copper, molybdenum and
uranium . Sibbald et al.
(1976) have suggested that these represent syngenetic
concentrations remobilized
during the Hudsonian orogeny. In addition, the Key Lake
uranium-nickel mineraliza-
tion is a s s oc iated with graphitic metasediments in the lower
part of the basal
sequence (Ray, 1976; Dahlkamp and Tan, 1977).
(b) Quartzite members of the basal succession carry zinc-lead
minera lization. This
t ype of mineralization is apparently r es tricted t o the Sito
Lake a nd George Lake
areas( ? regional zoning).
* DMR Assessment File 64El2NW004
-
- 102 -
The origin of these deposits remains controversial. Harper
(1975) drew attention
to the similarity between the Sito Lake occurrences and the
Eocambrian deposits of
Scandinavia (e.g . Laisvall, Vassbo) which have been described
by Grip (1967, 1973).
Other occurrences of this type include the Triassic deposit of
Largenti1 re, France
(Foglie"rini et al., 1965; Samama 1968), the Cretaceous deposits
of Bou-Sellam,
Morocco and Kroussou, Gabon (Caia, 1976) and the Carboniferous(
?) deposit of Cape
Breton Island, N.S. (The Northern Miner, March 3, 1977).
Samama (1968) proposed a syngenetic-sedimentary model for the
Largentiere
deposit, in which heavy metals are derived from the Hercynian
basement during the pre-
Triassic weathering cycle.
Lead isotope data for galenas from the Wollaston domain
(Cumming~ al., 1970;
Sangster, pers. COlID!I . , 1976) yield a two stage model which
supports the theory that
lead derived from Archean basement was deposited in Aphebian
metasediments.
Within the constraints of such a model, regular tabular
mineralized zones would
probably be an exception. Such features as paleotopography,
paleochannels, presence
of argillaceous interlayers, etc. would act as controls to
produce zones of complex
geometry.
(c ) At the southern end of the Wollaston domain, in the
vicinity of Duddridge Lake,
the base(?) of the Wollaston Group is marked by a thick sequence
of quartzites and
meta-conglomerates. Uranium-copper-vanadium mineralization is
present within lenses
in carbonaceous quartzites. Sibbald et al. (1976) suggest that
this occurrence may
represent an Aphebian Colorado Plateau-type deposit.
(d) Meta-conglomerate- and meta-arkose-hosted chalcocite-native
copper mineraliza-
tion in the Kaz Lake area appears to be unrelated to local
structural features,
igneous rocks or alteration of host rocks. The primary control
may be stratigraphic.
Chalcocite-native copper mineralization is characteristic of
red-bed environments
(e.g. Tourtelot and Vine, 1976). The host rocks in the Kaz Lake
area are commonly
pink to grey meta-arkoses, that contain variable, but
ubiquitous, amounts of hematite
and magnetite. Various authors (e.g. Rose, 1976) have emphasized
the spatial asso-
ciation of red-bed copper occurrences and evaporites; within the
Kaz Lake area
calcareous meta-arkoses, calc-silicates and marbles occur. It is
possible that
evaporites have not been recognized.
The as sociat ion of copper and lea d in mineralized boulders
within the Kaz area
presents a problem worthy of further s tudy . I t is not clear
wh ether this as socia-
tion represents a possible Cu-Pb-Zn r egi onal zoning, or is a
locali zed Cu-Pb sulphide
facies variation within an areally restricted basin
environment.
-
- 103 -
The chalcopyr ite-mol ybdenite bearing boulders hsve not been
traced t o a sour ce
(other than molyb denum mineralization at Mud Lake, Fig. 1) but
it i s i nteresti ng to
note that these boulders may have been derived froo a widespread
'source bed' t hat
i s part of the upper calcareous meta-arkoses and calc-silica
tes of the Wolla ston
Group.
In conclusion, the importance of boulder tracing cannot be over
emphasized. A
large number of the base metal occurrences within the Wollaston
domain have been dis-
covered through this method; and the use of geochemical methods
is conspicuous by i ts
absence. I n telligent geochemical til l and overburden s
ampling could pr ovide a suitable
s c ientific alternative to t he rapidly declining era of the
methodical prospector.
References
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ls of Copper, Lead , and Zinc Mineralizations in the Lower Cre t
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422.
Chadwick, B. (1968): The Geology cf the Morell Lake Area (West
Half ) , Saskatchewan ; Sask . ~ept. Min. Res ., Rept . 116.
Cumming, G.L. , Tsong , F. , and Gudjurgis, P. J. (1970):
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and Scott., B. ( 1976) : Rb /Sr dating of r o.cks from the
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Dahl k.amp, F.J. and Tan, B. (1977): Geol ogy and Mineralogy of
the Key Lake U-Ni Deposits , Northe rn Saskatchewan. Symp. Geology
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Karup-Moller, S. (1 970): Geology of the Compuls ion River Fold
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