Download A Re-examination of the Context of U

A Re-examination of the Context of U-Cu, Cu, and U Mineralization,
Duddridge Lake, Wollaston Domain 1
G.D. Delaney
Delaney, G.D. (1993): A re-examination of the context of U-Cu, Cu, and U mineralization, Duddridge Lake, Wollaston Domain; in
Summary of Investigations 1993, Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 93-4.
During a five week period in the summer of 1993,
1: 1O 000 scale mapping was completed of a 30 km2
area between Duddridge Lake and Walsh Lake, in the
south-central part of the Sandfly Lake mapsheet-area
(NTS 730-9). The area comprises a north-northeasttrending strip along the eastern margin of the Wollaston
Domain, and flanks the unconformable eastern contact
of supracrustal rocks with a heterogeneous granitoid terrane containing supracrustal remnants (Figure 1). The
purpose of this investigation was to re-examine the stratigraphic and structural context of the sediment-hosted
Thor U-Cu showing as well as other types of mineralization in the Duddridge Lake area. This work will provide
a starting point for a re-evaluation of the stratigraphic
and sedimentological context of base metal mineralization in supracrustals of the Wollaston Domain.
1. Previous Work
In 1949, Frarey (1950) undertook reconnaissance geological mapping of the lie-a-la-Crosse area. During the
summer of 1962, Money (1965) mapped the Duddridge
Lake area as part of a three year program of 1:63,360
mapping of the Sandfly Lake (east half-730-9), Black
Bear Island Lake (west half-73P-12), and Eulas Lake
(west half-73P-13) map areas. This mapping also
formed the basis for Money's Ph.D. dissertation entitled
"The Precambrian geology of the Needle Falls area",
completed at the University of Alberta in 1967.
On the basis of fieldwork during the summer of 1974,
and a compilation of known geological information, Munday (1974, 1978) prepared a 1:100 000 compilation
map of the geology of the Precambrian Shield rocks of
the eastern part of the lie-a-la-Crosse map-area. In
1975, Haughton (1976), of the Saskatchewan Research
Council, completed a multi-media geochemical survey
of the area containing the mineralized boulder train associated with the Thor Cu-U showing at Duddridge
Lake. In 1976, Bretzlaff completed a B.Sc. thesis entitled "Genesis of uranium mineralization at Duddridge
Lake, Saskatchewan". In 1978, Coombe and Potter
mapped a strip from Duddridge Lake northeast to Meyers Lake at a scale of 1:50 000 (Coombe, 1978b). This
work formed part of a study of base metals in the Wollaston Domain (Coombe, 1977, 1978a, 1979, in prep;
Coombe Geoconsultants, 1991 ). Also in 1978, the Saskatchewan Research Council studied the geochemistry
of basal till down ice from the Thor Cu-U showing
(Sopuck and Lehto, 1979). The economic geology section of this report summarizes several mineral exploration programs which have also taken place.
2. Regional Geological Setting
The Duddridge Lake area lies near the eastern side of
the Wollaston Domain (Figure 1; Lewry and Sibbald,
1977), a northeast-trending, generally tightly folded linear belt of siliciclastic metasediments and minor metavolcanics mantled and segmented by interfolded remobilized Archean granitoids (Money, 1968; Money et al.,
1970; Ray, 1979; Lewry and Sibbald, 1979, 1980; Ray
and Wanless, 1980; Lewry, 1981; Stauffer, 1984). The
domain has been classified as the easternmost lithostructural subdivision of the Cree Lake Zone which is interpreted to have "evolved by thermally driven remobilization of Archean continental basement and Aphebian
shelf-miogeoclinal cover" (Lewry and Sibbald, 1980,
p74).
The Wollaston Domain is bounded on the east by the
Needle Falls Shear Zone (Munday, 1974; Ray, 1974;
Stauffer and Lewry, 1988), a fundamental crustal structure (Lewry and Sibbald, 1980). Although metamorphic
grade is lower amphibolite facies in places along the
western boundary, the grade increases rapidly to the
west to upper amphibolite-granulite facies (Munday,
1978; Lewry et al., 1978). The western boundary is with
the Mudjatik Domain, which forms the high-grade core
of the Cree Lake Zone, and is marked by a change in
structural style from linear to arcuate. Compositionally
heterogeneous granitoids predominate and supracrustal
rocks, although in structural continuity with those of the
Wollaston Domain, are subordinate (Lewry and Sibbald,
1980).
Throughout much of the Wollaston Domain two main
episodes of deformation are distinguished (op cit). The
first event (01) formed a prominent foliation that is typically parallel to original layering and is interpreted to
have paralleled the basement cover contact. The second major distinguishable event refolded 01 structures
into tight northeast-trending, commonly doubly plunging
folds. As this corresponds to D3 deformation in the adjacent Mudjatik Domain, that designation was applied in
the Wollaston Domain. Other, generally minor, post 03
deformations are recognized locally such as in the Duddridge-Meyers Jakes area (Coombe, 1978b), the Pen-
(1) Saskatchewan Project A.12b was funded in 1993 under the Canada-Saskatchewan Partnership Agreement on Mineral Development 1990-95.
Saskatchewan Geological Survey
73
. ., •.
. 105" ·
ATHABASCA
58°
BASIN
40
km
Legend
Moior pluton
Undivid ed gronit oids
r::-:3
Sand stone / con g lomer ale
~ A th abasca 8osin
FT1
Ark ose / congl ometote
L::.2i,J Woll os ton
~==~=~
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Pelite Wolloston
Greywock e, pelite
semi pe!i ,e
Figure 1 - Major /ithostructural elements in the central part of the Precambrian shield of northern Saskatchewan (modified after
Macdonald and Broughton, 1980).
74
Summary of Investiga tions 1993
delton Lake area (Scott, 1973), and the Hidden Bay
area (Wallis, 1971).
3. General Geology
With the exception of areas to the east of Walsh Lake
and west of the narrows on Duddridge Lake, outcrop is
generally sparse because of thick glacial cover. The
dominant structural grain in the Duddridge Lake area is
north-northeasterly. The eastern part of the area is underlain by a heterogeneous granrtoid terrane that includes monzodiorite, felsite, granite, and diorite; locally
there are abundant xenoliths of biotite granulite and
gneiss.
The granitoids are overlain unconformably to the west
by the Meyers Lake Group, a thick succession of siliciclastic sediments. This sequence includes a basal
quartz pebble conglomerate which is overlain by quartzite. This is followed by a thick sequence of arkose, conglomerate, and grit with intercalated pelites. Despite evidence of multiple deformations, such as small scale
folds and strike parallel high-strain zones, this sedimentary sequence appears to essentially young to the west
with only minor structural repetition. There is an abrupt
rise in metamorphic grade to the west resulting in recrystallization and obliteration of original textures and
structures.
Carbonaceous-bearing lenses in hematitic arkose within
the arkose sequence host uranium-copper mineralization at the Thor showing. Minor copper mineralization
also occurs in the same red bed arkosic sequence.
Anomalous radioactivity is also associated with the basal quartz pebble conglomerate and some pegmatites.
4. Descriptions of Rock Types
a) Older Supracrustal Rocks
Xenoliths of supracrustal rocks occur in the granitoids
that underlie the east part of the area (Figure 2).
Among these xenoliths, hornblende blotite granulite and
schist are more abundant than biotitic quartzofeldspathic gneiss.
Hornblende-biotite Granulite and Schist (unit HBS)
Xenoliths of fine-grained to less commonly mediumgrained, dark grey hornblende biotite granulite and
schist occur north of Duddridge Lake. Xenoliths range
in size from a few centimetres in diameter to several
hundred metres in length, such as the conformable
body 1.5 km east of the south end of Walsh Lake which
is over 100 m wide and several hundred metres long.
Unit HBS is composed of 40 to 45 percent biotite, 15 to
30 percent hornblende, 20 percent plagioclase, 10 to
12 percent quartz and minor epidote, sphene, and magnetite. Locally there are abundant foliated leucocratic
quartz-feldspar veins.
migmatitic derivatives east of the supracrustals. In the
northeastern extension of the granitoids in the Hewetson Lake map area, lenses, layers, and xenoliths of amphibolite are common (Ray, 1981). The unit HBS xenoliths are probably the remnants of volcaniclastic rocks.
Quartzofeldspathlc Gneiss (unit QFN)
To the east of the large island at the north end of Duddridge Lake, enclaves of fine-grained, pink to buff
weathering, compositionally layered, biotitic quartzofeldspathic gneiss occur in felsite. These xenoliths might be
derivatives of immature quartzofeldspathic sediments or
volcaniclastics.
b) Younger Supracrustal Rocks: Meyers Lake
Group
Quartz Pebble Conglomerate (unit QC)
A sequence containing quartz pebble conglomerate occurs at the western contact of the granitoid terrane (Figure 2). Unit QC varies in thickness from 2 to 3 m on the
large island at the north end of Duddridge Lake to approximately 40 m east of Walsh Lake. Previous authors
traced this unit for another 35 km north-northeast of the
current mapping (Money, 1965; Coombe, 1978b).
Money (1965) estimated that this unit has an apparent
thickness of 30 to 122 m; in contrast, Coombe reported
typical thicknesses of 35 to 50 m. At one location on
the west limb of a syncline near Webb Lake the apparent thickness is about 400 m (Money, 1965) and at
other localities the conglomerate is absent. On the basis of the degree of flattening of quartz pebbles Money
( 1965) calculated that the original thickness of this unit
was probably one and one half to three times the current thickness.
The quartz pebble conglomerate is characterized by an
intact to disrupted framework of milky to smoky quartz
pebbles. Although no granitic clasts were noted,
Coombe (1978b) observed that these become progressively more abundant to the north. Beds, typically less
than one metre thick, are broadly lenticular on a scale
of metres to tens of metres; some exhibit apparent normal grading. Locally coarse porphyroblasts of microcline are abundant. Intercalated with the quartz pebble
conglomerate are thin to medium beds of quartzite, grit,
conglomeratic quartzite, and biotite schist. Some of the
quartzite and grit beds are trough cross laminated, although even, parallel laminations are more common.
Both Coombe (1978b) and Munday (1978) observed fining upward cycles defined by beds of quartz pebble conglomerate overlain successively by cross-bedded quartzite, structureless sandstone, and argillite. Cross-bedding, scour surfaces, and normal grading consistently indicate that tops are to the west. On a formation scale
this unit also fines upward. On the southeast side of
Duddridge Lake, scarce anhedral porphyroblasts of garnet occur in the matrix of the conglomerate; in contrast
these porphyroblasts are abundant in lenses of intercalated biotite schist.
Unit HBS is correlated with those parts of Money's
(1965) unit 2, consisting mostly of hornblende-biotite
gneiss and granulite, that occur in the granitoids and
Saskatchewan Geological Survey
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UnconforMity
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Figure 2 - Geological sketch map of the Ouddridge Lake area.
76
Summary of Investigations 1993
In exposures on the southeast side of Duddridge Lake
and on the large island at the north end of the lake, the
contact between the quartz pebble conglomerate and
granitoids is covered. To the north of Duddridge Lake
the contact is commonly masked by a high-strain zone.
Rocks in this high-strain zone typically weather pink to
salmon and have high-magnetic susceptibility. At one locality 2.3 km north of Duddridge Lake (UTM co-ordinates 430330m E, 6161370m N) the basal quartz pebble conglomerate bed displays a scoured contact with a
large xenolith of melanocratic biotite-hornblende gneiss
in monzodiorite. Although other workers (i.e. Munday,
1978) have postulated that the quartz pebble conglomerate marks an unconformity, this observation definitively
supports this relationship.
Quartzite (unit Q1)
There is a gradational contact between the uppermost
bed of quartz pebble conglomerate and an overlying sequence of quartzites containing subordinate muscovite
schist and laminated argillite (unit 01). This unit ranges
in thickness from 37 m on the southeast side of Duddridge Lake to about 460 m at the north end of the map
area. Regionally, 01, which has a similar geographic
distribution as unit QC has been estimated by Money
{1965) to be between 460 and 610 m thick, and by
Coombe (1978b) to be 300 m thick.
Unit 01 is characterized by cream, buff or light grey
weathering, medium to thick beds of fine-grained quartzite commonly in packets of several beds. Many of these
beds are massive or parallel laminated. Cross-bedding
is rare. Quartzite beds alternate with layers of light
greenish grey biotite-muscovite schist containing laminae and lenses of quartzite. Coombe (1978b, p101) observed that "cyclical units in this part of the succession
are 15 to 25 m thick and comprise a basal massive
quartzite overlain by quartzite and intercalated schists
capped by a thin schist layer". Rare beds of quartz pebble conglomerate are intercalated in this sequence.
Some thick beds of glassy quartzite occur near the
base of 01. Locally actinolite is concentrated along foliation planes in the quartzite. Intercalated within the
quartzite-biotite-muscovite schist succession are intervals of brownish grey weathering. compositionally layered biotite-muscovite argillite-siltrte. One of these intervals forms a prominent marker horizon in 01 north of
the map area (Coombe, 1978b).
In a few outcrops, some of the more micaceous layers
are cut by a northeast-trending crenulation cleavage
that dips steeply to the west. Locally the sequence is
deformed into tight small-scale folds that generally dip
moderately to rarely steeply to the southwest and or
rarely to the northeast. Primary structures such as
cross-bedding and scour surfaces, common near the
base of 01, consistently indicate tops to the west.
The lower contact of unit 01 is placed at the top of the
uppermost bed of quartz pebble conglomerate. Rare exposures indicate that on the west side 01 typically
grades into a sequence of biotite schist and plagioclase
porphyroblastic biotite schist.
Saskatchewan Geological Survey
Biotite Schist (unit BS1)
A thick interval of biotite schist underlies the west side
of Duddridge Lake. Other than in a few outcrops at the
south end of Walsh Lake and one outcrop on the east
side of Poulin Lake, this unit is known only from diamond drill core (SEM Assessment Files 7309-0012 and
-0016). At the south end of Duddridge Lake the biotite
schist is apparently intercalated with biotitic quartzofeldspathic gneiss. The schist is typically dark grey to
black, strongly foliated, and locally crenulated. Single
grains or clots of magnetite occur locally.
Plagioclase Porphyroblastic Biotite Schist (unit BS2)
Unit BS2, which comprises plagioclase porphyroblastic
biotite schist and biotite schist occurs in a northeasttrending belt that extends from the north end of Duddridge Lake to the northeast side of Walsh Lake
(Coombe, 1978b). Diamond drilling revealed that this
unit also underlies the north part of Duddridge Lake
(SEM Assessment File 7309-0016). Apparent thickness
varies from about 80 to 120 m. Another large belt of
882 has been traced from the Churchill River to 3.3 km
north-northeast of Brunning Lake where it pinches out
(Money, 1965; Coombe 1978b). This unit also forms a
subordinate component of the thick interval of biotite
schist (unit BS1) lying west of Duddridge Lake. Other
smaller bodies of this unit have also been observed.
The schist weathers grey to dark grey, and contains
abundant, foliation flattened and rotated medium- to
coarse-grained porphyroblasts of plagioclase in a matrix
of biotite and less commonly minor hornblende. Diamond drilling under Duddridge Lake, on the strike projection of unit 882 at a location approximately 1 km
southwest of the north shore of the lake (UTM co-ordinates 428530m E, 6158660m N), intersected two intervals of plagioclase porphyroblastic biotite schist flanked
and segmented by pyritic biotite schist that includes
some carbonaceous material (SEM Assessment File
7309-0016).
Biotite-muscovite Schist (unit MS1)
A large body of biotite-muscovite schist underlies the
west side of Duddridge Lake. This unit pinches out on
the north side of Duddridge Lake and continues south
of the map-area. Biotite-muscovite schist is also intercalated in arkosic facies (units A1a to A1f) but the layers
are generally too thin to be indicated on the map. Although MS1 has an apparent thickness of as much as
500 to 600 m, a true estimate is hard to accurately determine, because locally pegmatite comprises as much
as 50 to 60 percent of the section. Local structural complications further hinder accurate thickness determinations.
The schist is typically a grey to buff grey, fine- to medium-grained rock containing foliae of mica, one or two
grains thick, in a quartzofeldspathic matrix. Muscovite
and biotite typically compose about 20 percent of the
rock. Locally the schist is compositionally layered. This
unit is typically crenulated; crenulations are axial planar
to small scale folds. Millimetre-thick, medium- to coarse-
77
grained quartz-feldspar veinlets, aligned parallel to foliation, are common and are boudinaged locally. Unit MS1
weathers various shades of grey to brownish grey;
some foliae and fracture surfaces are coated with limonite and or hematite.
places the biotite is distributed fairly uniformly on the
outcrop scale; elsewhere the biotite content occurs in
layers. This is a strongly foliated rock; locally the foliation is crenulated and folded. The biotitic quartzofeldspathic gneiss typically weathers buff to buff light grey.
Biotite-muscovite Schist with Intercalated Sandstone (unit MS2)
Homogeneous Quartzofeldspathic Gneiss (subunit A 1c)
Within the biotite-muscovite schist (unit MS1) there are
intervals that contain thin to medium beds of buff to
light grey weathering, fine-grained sandstone that alternate with laminae and thin beds of biotite-muscovite
schist and siltite. The thicker sandstone beds are typically dissected by numerous grey quartz veins.
Arkose, Conglomerate, Quartzofeldspathic Gneiss
and Grit (units A1a to A1f)
Arkose, conglomerate, grit, and metamorphic derivatives of these rocks form a significant component of the
succession to the west of the quartzite. Many of these
units have gradational contacts both laterally and vertically. Six subunits, A 1a to A 1f, are distinguished.
Conglomerate-Heterogeneous Quartzofeldspathic
Gneiss (subunit A1a)
Conglomerate and banded quartzofeldspathic gneiss, interpreted to be derived from the conglomerate, are exposed in small isolated outcrops on the west side of the
biotite-muscovite schist. The banded quartzofeldspathic
gneiss predominates farther to the west. This unit appears to be intercalated with other facies including grit
and biotitic quartzofeldspathic gneiss.
Conglomerate beds as much as a few metres thick, are
characterized by an intact to disrupted framework of
variably flattened buff to pink quartzofeldspathic clasts
of pebble to cobble-size. Conglomerate beds alternate
with intervals of homogeneous arkose.
The banded quartzofeldspathic gneiss is a strongly foliated, banded, light grey to pinkish light grey, fine- to medium-grained rock composed predominantly of quartz
and feldspar, and minor muscovite and biotite. Banding
is defined by pink to salmon, fine-grained, sharply
bounded, feldspar-rich lenses typically a few millimetres
thick and up to a few centimetres long. Banded intervals alternate with those of homogeneous quartzofeldspathic gneiss. The banded gneiss commonly weathers
a mottled pinkish buff to pinkish light grey. In exposures
where foliation is not as strongly developed, the feldspar-rich lenses are unequivocally leucocratic granitoid
clasts forming an intact to disrupted framework. This
unit contains disseminated hematite locally.
Biotitic Quartzofeldspathic Gneiss (subunit A 1b)
This unit, which occurs to the west of Duddridge Lake,
is intercalated in a variety of the other quartzofeldspathic facies and at least locally appears to have a gradational contact with biotite schist. The rock is typically
strongly foliated with 5 to 1 5 percent biotite disseminated in a framework of quartz and feldspar. In some
78
Unit A 1c is a strongly foliated, salmon coloured to light
grey-weathering, fine- to medium-grained quartzofeldspathic rock which is generally compositionally and texturally homogeneous on the outcrop scale. Locally this
subunit contains scattered leucocratic granitoid clasts
and rare feldspar prophyroblasts. Parts of subunit A 1c
contain disseminated fine- to medium-grained hematite.
Arkose and Feldspathic Quartzite (subunit A td)
A thick interval of this unit is well-exposed to the east of
Walsh Lake. The arkose, which is light grey to more
typically mottled pinkish buff weathering, includes parts
with primary laminae, including rare cross-laminae as
well as foliated homogeneous intervals. Locally there
are scattered leucocratic granitoid pebbles. Biotitequartz-feldspar pegmatites, some in excess of 30 m
thick measured perpendicular to the main regional foliation, are locally abundant. Preliminary thin section examination reveals that the arkose is composed of a finegrained interlocking mosaic of quartz, microcline, and
plagioclase with minor biotite and muscovite.
Grit (subunit A 1e)
Mappable intervals of grit overlie plagioclase porphyroblastic biotite schist east of Walsh Lake and occur
along the western contact of muscovite-biotite schist
west of the narrows in Duddridge Lake. Grit also forms
beds in subunits A 1d and A 1f. The grit overlying the plagioclase porphyroblaslic schist is a buffish pink to buffish light grey weathering, fine-grained quartzofeldspathic rock containing scattered, generally round, grey to
dark grey quartz grains typically a few millimetres in diameter. Less commonly, medium-grained porphyroblasts of plagioclase occur in the quartzofeldspathic
matrix. Grit along the west contact of the muscovite-biolite schist is compositionally similar although quartz
granules have been tectonically flattened and locally
are extremely ribboned out.
Conglomeratic Argilfaceous Arkose and Grit (subunit
A1f)
This subunit comprises pink, wavy thin beds and laminae of argillaceous arkose that contain rare dark grey biotite-rich rip-up clasts. Within this subunit are thin layers
composed of up to 20 percent scattered, pink, finegrained, leucocratic granitoid pebbles 1 to 3 cm in diameter. Beds as thick as 1 m contain about 20 percent
scattered, dark grey quartz grains up to 6 mm in diameter in a fine-grained quartz-feldspar matrix. Conformable
epidote-rich lenses occur locally and some exposures
contain disseminated hematite and weather a deep
salmon colour.
Summary of Investigations 1993
c) Granitoids
Pegmatite (unit P1)
The granitoid terrane east of the quartz pebble conglomerate is composed of a variety of rocks that locally contain abundant supracrustal enclaves.
Pegmatite occurs in all granitoid and supracrustal rocks
in the area. It is most abundant in the younger supracrustal units, particularly in biotite-muscovite schist
and meta-arkose. There are both compositional and textural variations of pegmatite and probably more than
one generation. In the biotite-muscovite schist, pegmatite is commonly a pink to grey weathering rock composed of two textural components: 1) medium- to
coarse-grained equigranular, and 2) very coarsegrained porphyritic. Pegmatite typically occurs in bodies
aligned parallel to foliation and range from a few centimetres to a few tens of metres in width and from a few
metres to tens of metres in length. Contacts vary from
sharp to gradational and some pegmatites are joined by
veins cross-cutting foliation. The pegmatites are composed of quartz, potassic feldspar, plagioclase, biotite,
and minor muscovite. Some pegmatites in biotite-muscovite schist contain clots of coarse-grained, black tourmaline. Pegmatites in biotite-muscovite schist at the
south end of Duddridge Lake are deformed into boudins
and there is commonly a reaction rim between the
boudins and adjacent pelites.
Feldspar Porphyroblastic Monzodiorite and Quartz
Monzodiorite (unit MD)
On the north and east sides of Duddridge Lake, as far
as 500 m south of the large island at the north end of
the lake, the main granitoid is a salmon to buff coloured, medium- to coarse-grained monzodiorite to
quartz monzodiorite containing coarse-grained porphyroblasts of microcline and approximately 20 percent medium- to coarse-grained clots of hornblende variably replaced by biotite. Foliation is locally very strong, particularly along the contact with the quartz pebble conglomerate, but is more typically weak to moderate, and a
strong lineation is common. The unit is cut by millimetrethick shears.
Felsite and Leucogranite (unit fel)
Felsite and leucocgranite are significant in the granitoid
terrane east of the quartz pebble conglomerate. To the
north of Duddridge Lake, salmon coloured felsite veins
and small irregular bodies cut the monzodiorite. To the
east of Duddridge Lake salmon to pink, fine-grained felsite to leucogranite are composed of 40 to 50 percent
quartz, 20 to 25 percent potassic feldspar, 20 percent
plagioclase, and 5 to 7 percent disseminated finegrained biotite. This unit, like other granitoid phases on
the west side of Duddridge Lake, is so poorly exposed
that its form and dimensions are masked.
Diorite (unit D1)
Diorite underlies the east side of the large island in the
north end of Duddridge Lake (Figure 1) as well as adjacent parts of the mainland to the east. The diorite is a
massive to weakly foliated, grey, medium- to coarsegrained rock composed of 20 to 35 percent hornblende,
variably replaced by biotite, in millimetre-size aggregates. Millimetre-thick shear zones cross-cut the weak
foliation.
Hornblende Porphyroblastic Diorite (unit D2)
West of Duddridge Lake, the biotitic quartzofeldspathic
gneiss is cut by a small body of dark green, mediumgrained melanocratic diorite that locally contains coarsegrained porphyroblasts of hornblende.
Granite (unit G1)
Foliated to massive, salmon coloured to pink, mediumgrained granite occurs throughout the granitoid terrane
east of the quartz pebble conglomerate. This rock typically contains 7 to 12 percent fine-grained biotite, commonly in clots. Locally there are phenocrysts of potassic
feldspar. The most extensive body of granite occurs on
the southeast side of Duddridge Lake .
Saskatchewan Geological Survey
Granodiorite (unit GD1)
This unit and granite (unit G1) constitute the two main
granitoid phases on the southeast side of Duddridge
Lake at the contact with the quartz pebble conglomerate. The granodiorite is a grey to buff grey, fine- to medium-grained rock composed of 35 to 40 percent smoky
quartz, 15 percent potassic feldspar, 35 to 40 percent
plagioclase, and 7 percent biotite. This rock is weakly foliated and locally contains a strong lineation.
5. Depositional Setting of the Meyers
Lake Group
The quartz pebble conglomerate (unit QC) is interpreted
to have been deposited in the medial to distal parts of a
laterally extensive and unconfined braid plain (Rust and
Koster, 1984). Formation of this extensive apron of mature siliciclastic sediment marked the initiation of rifting
along a zone that broadly corresponds to the Needle
Falls Shear Zone (Coombe, 1979; Ray, 1979). The initial phase of uplift, associated with rifting, probably unroofed previously deposited mature siliciclastic sediments (cf. Money, 1965). The area between Duddridge
and Meyers Lake is considered to represent one of a
number of initially closed basins that typically develop
along extensive rift systems (Jowett, 1989).
The quartzite (unit 01) is interpreted to have been deposited during pulses of upper flow regime sediment
laden surges in broad channels in progressively more
distal parts of the braid plain apron. Continued transgression resulted in deposition of pelitic sediments, represented by biotitic schist and plagioclase porphyroblastic biotite schist (unit BS 1), over the braid plain apron.
Reactivation of the rift zone is then considered to have
produced new pulses of immature coarse elastic sedimentation along the rift margin depositing arkose, conglomerate, and grit in proximal settings, and pelites and
79
semi-pelites farther away from the main sediment dispersal points. Subsequent alteration of some of the
coarse elastic sediments would then have produced redbeds and created local enrichments in uranium and copper as well as associated elements (Coombe, 1979).
In this section, a review of exploration history and develop'!le.nt for the Duddri~ge Lak~ area is followed by a descnpt1on of the geological setting and characteristics of
the occurrence types.
a) Exploration History and Development
6. Structural Geology
!n the summer of 1974, Kole Lovang, a prospector work-
The structural history of the Duddridge Lake area appears to be similar to that documented for the Duddridge- Meyers lakes area by Coombe (1978b). Bedding, laminations, and other primary features, such as
cross-bedding, grading, and scour surfaces, are well
preserved in the quartz pebble conglomerate and
quartzites adjacent to the unconformity with granitoids.
These structures consistently indicate that the sequence youngs to the west. To the west, primary structures are progressively obliterated so that only in rare instances, such as locally in the arkoses on the southeast
side of Walsh Lake, are primary features such as crossbedding preserved. Where present, these also consistently indicate tops to the west.
ing on behalf of Thor Exploration Limited, discovered a
train of uraniferous carbonaceous arkose boulders on
the west side of Duddridge Lake. Claims in the area
were acquired by Thor, Mark V Petroleums and Mines
and Brascan. Shortly thereafter, joint venture agree- '
ments were concluded between these companies and
Noranda. Subsequent follow-up of the Thor showing in
late 1974 and early 1975 included linecutting, geological mapping, boulder sampling, ground magnetometer
and radiometric surveys (SEM Assessment File 73090007) and a 21 hole diamond drilling program totalling
2477.4 m. This drilling defined a 61 O m long zone of
uranium mineralization of limited width and grade (Figure 2). In 1975, additional geological, geochemical, and
geophysical follow-up work was completed in the area
o~ _the origin~I showing as well as regionally, and an add1t1onal 11 diamond drill holes totalling 728.7 m in
length were drilled on the Thor prospect. On the basis
of the combined drilling, two ore zones have been defined with a combined tonnage estimated at 357,310
tons grading 2.11 lbs/ton U30s (SEM Assessment File
7309-0012).
A strong foliation, S1, developed throughout the area
generally trends northeasterly, and parallels bedding. In
rare exposures, such as in one outcrop of meta-arkose
southeast of Duddridge Lake, S1 was observed to be
axial planar to small-scale isoclinal folds.
A second foliation, S2, occurs locally in the siliciclastic
supracrustals, but in many places it is hard to distinguish between S1 and S2. The trend of 82 varies from
nort~-~orthwesterly to commonly north-northeasterly,
and ti ts apparently axial planar to folds with a maximum wavelength of a few metres that plunge moderately to the northeast or southwest. Unlike the documented instances found farther to north (Coombe,
1978b), no large scale examples of these structures
were encountered.
North-northeast-trending high-strain zones are also attributed to 02 deformation (Coombe, 1978b). Examples
of these high-strain zones occur in the grit unit on the
west contact with the biotite-muscovite schist west of
!he narrows_on Duddridge Lake and between the quartzite and plag1oclase porphyroblastic biotite schist north of
Duddridge Lake.
The latest structures recognized in the Duddridge Lake
~rea are ve~ica~ ?renulation cleavages common in pelit1c and sem1-peht1c rocks. These steeply dipping structures appear to be aligned in two distinct trends: easterly and north-northeasterly.
7. Economic Geology
Mineral occurrences in the Duddridge Lake area include: 1) the Thor U-Cu prospect; 2) U in pegmatites;
3) U-Th concentrations in the quartz pebble conglomerate at the base of the Meyers Lake Group; 4) elevated
Cu concentrations in a variety of contexts in the arkose
of the Meyers Lake Group; and 5) oxide facies iron formation float/drift.
80
Regional work resulted in the discovery elsewhere of
anomalous concentrations of uranium and thorium in
the basal conglomerate of the Meyers Lake Group. A
0.3 to 0.45 m wide, 45.7 m long pyritic, micaceous sandstone lens containing anomalous uranium near Sandfly
Lake (SEM Assessment File 7309-0010) and a uraniferous albite-biotite pegmatite also near Sandfly Lake containing patchy concentrations of uranium assayed as
much as 1.5 lbs of U30s per ton over a width of 3 m, although most were significantly less (SEM Assessment
File 7309-0011) .
In ~ 976 the Saskatchew~n Mining Development Corporation became a partner in the Noranda-Brascan joint
venture. During that year geophysical and geochemical
surveys were focused on the area south of Duddridge
Lake. An additional 1O diamond drill holes totalling
565.7 m in length were drilled to test targets identified
during this work. No uranium mineralization was intersected. Subsequently the joint venture agreement was
terminated and the claim blocks encompassing the
showing and adjacent lands reverted to the original owners, Thor or Mark V.
In 1978, Thor continued work that included multi-media
geochemical surveys over four grids near Duddridge
Lake (SEM Assessment File 7309-0019); this was followed up with a 1980 basal till geochemical survey
north of the Thor prospect (SEM Assessment File 73090015) and a 1981 program of 10 diamond drill holes totalling 1610 m in length drilled in the north end of and
to the west of Duddridge Lake (SEM Assessment File
7309-0016).
Summary of Investigations 1993
In 1979, Mark V completed a magnetometer survey of
the Walsh Lake area (SEM Assessment File 73090021 ). Although Thor retained a mineral lease over the
U-Cu showing, adjacent claims lapsed until 1993 when
Noranda acquired a significant land holding in the area.
b) Descriptions of Mineral Occurrences
Thor U-Cu Prospect
Rock exposure is scarce in the vicinity of the Thor U-Cu
Prospect, which is only revealed as a mineralized boulder train. Consequently, information about the showing
and its context has been derived primarily from diamond drill holes. The following account is based on information contained in the Mineral Assessment Files of
Saskatchewan Energy and Mines, a report by Coombe
(1978b), thesis investigations by Bretzlaff ( 1976), and
preliminary petrographic and geochemical work by the
author.
Mineralization occurs in the structurally lower part of a
north-northeast-trending sandstone sequence which
dips moderately to steeply to the west. On the basis of
primary lithologic variations and alteration mineral assemblages, a number of subdivisions are recognized in
the sandstone. These include striped arkose comprising
alternating maroon and greenish light grey colour bands
(see Coombe 1978b); a micaceous sandstone containing 10 to 20 percent biotite, muscovite, and chlorite; a
hematitic arkose characterized by interstitial dustings of
hematite; a vuggy limonitic stained variety; and carbonaceous arkose.
Carbonaceous arkose, host to the uranium copper mineralization, is a light grey to buff light grey rock with
dark grey carbonaceous laminations and mottled areas.
"The uraninite is found either as separate grains dispersed throughout the sandstone ... or may be concentrated in aggregates along bedding, fracture or schistosity planes" (Bretzlaff, 1976, p14). In addition t~
uraninite, carbonaceous sandstone also contains chalcopyrite, pyrite, bornite , galena, pyrrhotite, sphalerite as
well as very rare molybdenite (op cit.). The carbonaceous arkose occurs as irregular lenses within hematitic
arkose. Two of the carbonaceous arkose lenses are
mineralized; others, however, are unmineralized. The
sandstone sequence is segmented and locally totally replaced by pegmatite. At the structural base of the sandstone sequence is a biotite schist.
Bretzlaff (1976, piii) attributed the Thor occurrence to
"epigenetic chemical precipitation of uranium from circulating ground waters in the local reducing environment
of the carbonaceous arkose". Lewry and Sibbald (1979)
noted the similarity between the Thor showing and uranium occurrences in sandstone in the Colorado Plateau
region. This showing, and the associated copper mineralization discussed below, are characterized by many
features typical of stratiform-hosted copper deposits associated with red beds formed in rift-settings (Kirkham,
1989; Brown, 1992). Coombe (1979) also noted the possible red-bed association of the showing.
Saskatchewan Geological Survey
U in Pegmatites
Some pegmatites in the Duddridge Lake area contain
anomalous concentrations of uranium. For example
Bretzlaff (1976) observed that some of the pegmatites
in sandstones near the Thor U-Cu showing contain
uraninite along veinlets. These pegmatites also contain
chalcopyrite locally. Elsewhere, prospecting between
Duddridge Lake and Needle Rapids led to the discovery
of a dozen outcrops or boulders of radioactive pegmatite (SEM Assessment Files 7309-0010). No economically significant grades are reported. Radioactive peg-.
matites in supracrustal rocks, particularly those associated with graphitic pelites, are common throughout the
Wollaston and adjacent Mudjatik Domains (Sibbald et
al. , 1977; Lewry and Sibbald, 1979).
U-Th in Quartz Pebble Conglomerate
Some of the beds of quartz pebble conglomerate in the
base of the supracrustal sequence contain anomalous
concentrations of uranium and thorium (SEM Assessment Files 7309-0009, -0010, and -0011 ). In a study of
radioactivity in an exposure of the conglomerate at the
south end of Duddridge Lake, Munday (1978) observed
surface radioactivities of up to 6 times background
caused by elevated concentrations of both U and Th. A
23 cm wide bed of quartz pebble conglomerate, that
was traced for 37 rn along strike, has 10 times background radiation. Although a grab sample from a trench
in this bed yielded 0.09 percent U30a, a bulk sample
from the trench contained only 0.005 U30a; Munday
also noted elevated concentrations of selenium and vanadium in the conglomerate (op cit).
Cu in Arkose
In addition to the Thor uranium-copper showing, the
sandstone sequence that hosts this mineralization also
contains other occurrences of minor copper mineralization. These include chalcopyrite-bearing fractures, chalcopyrite in quartz veins, pegmatite with stringers of
bornite and/or chalcopyrite, disseminated chalcopyrite,
and patchy mottled areas of bornite (SEM Assessment
File 7309-0016).
Oxide Facies Iron Formation Float
A rusty weathering, tabular, cobble-sized fragment of
magnetite-bearing iron formation was discovered during
mapping approximately 1 km north of Duddridge Lake
along the west side of a prominent valley underlain by
unit BS2 (UTM co-ordinates 429605m E, 6160720m N).
An assay revealed this rock contains 22.54 percent
iron. The friable nature of this boulder suggests it had
not been transported a great distance. A follow-up to
trace the source of this boulder is warranted.
81
8. Stratigraphy of Wollaston Domain Supracrustal Rocks, Duddridge Lake
Area
a) Review of Previous Ideas
A variety of stratigraphic classifications have been proposed for the supracrustal rocks in the Wollaston Domain (Saskatchewan Geological Survey, 1987). Even in
the southern part of the domain, which encompasses
the Duddridge Lake area, several different stratigraphic
classifications have been proposed and modified as
new data became available.
Money (1965) proposed the name Meyers Lake Group
for the basal quartz pebble conglomerate and overlying
quartzite sequence with intercalated pelitic schists and
suggested that this group unconformably overlies a sequence of "older metamorphic rocks" which he subsequently named the Sandfly Lake Group (Money,
1968). Money included in the Sandfly Lake Group metaarkose, hornblende-biotite rocks, amphibolite, biotite-plagioclase rocks, and acid metavolcanic rocks. The Sandfly Lake Group thus defined not only comprises most supracrustal units west of the quartzite, but also rocks to
the east, which Money (1965) postulated to be felsic volcanics, but which were subsequently identified by Munday (1978) as mylonites associated with the Needle
Falls Shear Zone.
In the Daly Lake area (Figure 1), approximately 110 km
north-northeast of Duddridge Lake and 20 km west of
the Needle Falls Shear Zone, Money (1966) also proposed the name Daly Lake Group for supracrustal
rocks containing a basal pelitic succession overlain and,
in part, intercalated with arkose, subordinate conglomerate and quartzite, and containing calc-silicate lenses.
Money noted this succession was regionally extensive
in the central part of the Wollaston Domain west of the
Needle Falls Shear Zone (Money, 1968; Money et al.,
1970).
In 1975, Ray, on the basis of re-mapping in the Foster
Lake (NE)-Geikie River (SE) area, concluded that
rocks previously mapped as correlative with the Sandfly
Lake, Daly Lake and Meyers Lake groups by Scott
(1973) comprise a single succession which he termed
the Wollaston Group.
On the basis of 1:100 000 scale remapping in 1974, of
the lie-a-la-Crosse (East) Map sheet, which includes
the Duddridge Lake area, Munday (1978) suggested
that Money's (1965) Meyers Lake Group, as well as
other siliclastic units to the west including arkoses, pelites and their metamorphic derivatives, which had been
formerly assigned to the Sandfly Lake Group, are all
part of the same sequence; the differences recorded in
these rocks are attributed to sedimentary facies
changes as well as variations in deformation style and
metamorphic grade. Munday also suggested that his
new expanded Meyers Lake Group could be considered a lithological variant of the Daly Lake Group
(Money, 1966).
82
Coombe, who mapped the area between Duddridge
and Meyers Lake area at a scale of 1:50 000, in 1978,
subdivided the supracrustal rocks into two unnamed
groups: one included biotitic rocks including biotite
schist and plagioclase porphyroblastic biotite schist; and
the other included the quartz pebble conglomerate,
quartzite, arkose, and biotite-muscovite schist.
In a 1979 paper, Ray (p24) proposed that the supracrustal rocks of the Wollaston Domain are ' separable into
two contrasting assemblages, a widely developed 'Wollaston Group' and a more restricted 'Needle Falls
Group' ... The Needle Falls Group is confined as thin
strips to the extreme southeastern margin of the Wollaston Domain, adjacent to the Needle Falls Shear Zone
and includes rocks formerly designated variously as the
Meyers Lake, Courtenay Lake, Sandfly Lake or Souter
Lake groups (Money, 1965; Money et al. 1970; Lewry,
1977)." These rocks, characterized by coarse elastic facies and locally intercalated mafic volcanics, he interpreted to have been deposited along a rift margin that
broadly corresponds to the Needle Falls Shear Zone
(Coombe, 1979; Lewry et al., 1981). In a 1979 paper
Coombe adopted Ray's twofold subdivision of the Wollaston supracrustals into the older Needle Falls Group
and younger Wollaston Group (see also Coombe Geoconsultants, 1991 ).
b) Present Author's Conclusions on Regional
Stratigraphic Relation of the Ouddrldge
Lake Area
Present mapping suggests that stratigraphic relationships in the Duddridge Lake area are as established by
Munday (1978), that is all supracrustal rocks west of
the granitoid terrane belong to one succession . Evidence for an unconformity in this sequence is equivocal. Similarly, re lationships with supracrustals in the
main part of the domain, the "Daly Lake Group", and
equivalent st rata are unclear.
Although on a broad scale coarse elastic facies are
common along the eastern margin of the Wollaston Domain (Coombe, 1979), there are sufficient distinctions
from area to area which seem to preclude lumping
them all into one stratigraphic unit such as the ' Needle
Falls Group". For example, in the George Lake area
(Figure 1). in contrast to the Duddridge-Meyers lakes
area, the sequence included in the Needle Falls Group,
Courtenay Lake Group (Scott, 1970), and Lower metaarkose (Coombe, 1978a) consists of a succession of
arkoses, conglomerates, and breccias containing two
horizons of amphibolite derived at least in part from
mafic volcanics. Elsewhere, such as in the Barnett Lake
area, rocks that would presumably be included in the
Needle Falls Group (Coombe, 1979) have been described by Money (1961) as arkose with intercalated
conglomerate; subsequently Ray (1975) reinterpreted
the meta-arkose as metamorphosed felsic volcanics
and the conglomerates as tuffaceous derivatives.
A similar argument could be made against including all
rocks in the central part of the Wollaston Basin in the
Wollaston Group, for again local variations in stratigraphy have been recognised.
Summary of Investigations 1993
By documenting and then comparing and contrasting regional variations in stratigraphy, a more detailed understanding of the character and evolution of the Wollaston
Basin should become apparent. Such an understanding
is also critical for understanding metallogenic relationships. Consequently I would advocate moving beyond
basin-wide stratigraphic classification schemes based
upon locally set up assemblage names, such as many
of those illustrated in the chart on page 16 of Saskatchewan Geological Survey (1987) or that by Coombe Geoconsultants (1991), to a three dimensional scheme of
fence diagrams that focuses on lithological regional variations. For the younger supracrustal succession in the
Duddridge- Meyers lakes area, I favor, as suggested by
Lewry (1981), abandonment of the all-encompassing
Needle Falls Group and return to the use of the term
Meyers Lake Group in the expanded context as defined
by Munday and in this report.
9. Economic Potential of the Wollaston
Domain
Many major Proterozoic sedimentary basins. like the
Wollaston, are host to a spectrum of economically significant mineral deposits in a variety of settings. As an
example, the rift formed Middle Proterozoic Belt Basin,
along the western side of North America, is host,
amongst others, to: the 160 million tonne Sullivan PbZn deposit (average grade of 5 percent Pb, 5 percent
Zn, and 2 ounces of silver per ton (Hamilton et al.,
1982); several sediment-hosted stratiform copper deposits, such as the 85 Mt Spar Lake deposit (average
grade of 0.76 percent Cu and 54 g Ag per tonne
(Hayes et al., 1989), and the stratigraphically controlled
lead, zinc, and silver veins of the Coeur D'Alene district,
which by the end of 1980 had already produced
935,287,000 ounces of silver, 7,679,772 tons of lead,
3,051,743 tons of zinc, 500,553 ounces of gold, and
160,985 tons of copper (Bennett and Venkatakrishnan,
1982).
Although the Wollaston Domain has received but a
small fraction of the exploration activity as the Belt Basin, a variety of mineral occurrences have been identified in Wollaston supracrustals. These include the sediment hosted copper in the Pendelton Lake area (Scott,
1973; Coombe, 1977); lead-zinc occurrences in the
George and Sito lakes area (Karup-Moller and Brummer, 1970; Coombe, 1977; Potter, 1977, 1978, 1980);
the Marina lead-zinc showing at Johnson Lake
(Coombe, 1977); and U-Cu mineralization at Duddridge
Lake (Bretzlaff, 1976; Coombe, 1978b). Although none
of these occurrences are presently economic, the diversity of mineralization types indicates a significant base
metal potential for the Wollaston Domain. This potential
has been furth er underlined by recent significant discoveries by Noranda (Northern Miner, May 24, 1993).
10. Acknowledgments
Kevin Fossenier is thanked for his invaluable assistance
during both the field and office portions of this investigation. Pam Schwann helped with mapping for one week.
Saskatchewan Geological Survey
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_ _ _ _ (1979): A review of pre-Athabasca basement geology in northern Saskatchewan; in Parslow, G.R. (ed.), Uranium Exploration Techniques, Sask. Geol. Soc., Spec.
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