Download Geology and Metamorphic Petrology of Variably Altered Volcanic

Geology and Metamorphic Petrology of Variably Altered Volcanic
Rocks in the Southern Reindeer Lake Area, Northern Saskatchewan
Donald M Wright
1
,
Kevin M Ansdell 1, David Corrigan 2 , and Ralf 0. Maxeiner
Wright, D.M., Ansdcll, K.M., Corrigan, D., and Maxeiner, R.O. ( 1999): Geology and metamorphic petrology of variably altered
volcanic rocks in the southern Reindeer Lake area, northern Saskatchewan; in Summary of Investigations 1999, Volume 2,
Saskatchewan Geological Survey, Sask. Energy Mines, Misc. Rep. 99-4.2.
The Reindeer Lake area has been the recent focus of
detailed lithological and structural mapping by the
Saskatchewan Geological Survey (Maxeiner, 1996,
1997, I 998, this volume) and the Geological Survey of
Canada (Corrigan et al., 1997, 1998a, l 998b, this
volume). Metamorphosed and altered volcanic rocks
and associated sedimentary rocks forming the
northeastern extension of the Central Metavolcanic
Belt were identified in the Reindeer Lake area
(Sibbald, 1977; Stauffer et al., 1979, 1980). These
rocks were subsequently subdivided into two belts by
Maxeiner (1997), called the Reed Lake and Lawrence
Point volcanic belts, and continue to be refined
(Maxeiner, this volume). Corrigan et al. (l 998a, this
volume) recognized volcanic and sedimentary rocks,
including iron formation, in the Laxdal-Doucet islands
area, and interpreted these as a northern extension of
the La Ronge Domain. The purpose of this ongoing
study is to characterize the petrology and metamorphic
paragcnesis of all these supracrustal rocks, as well as to
determine their possible protoliths and depositional
environment.
1. Regional Geology
The study area is located in the La Ronge Domain,
which was accreted to the margin of the Archean
Hearne craton prior to terminal collision at ca. l.83 Ga.
(Bickford et al., 1986; Lewry et al., 1990). The La
Ronge Domain is thrust onto the Kisseynew Domain to
the south (Figure l ), which comprises the highly
deformed and metamorphosed rocks of the Bumtwood
Group and the structurally overlying Sickle-McLennan
elastic sediments (Johnston and Thomas, 1984,
Corrigan et al., 1999). The La Ronge Domain is
flanked to the north by the Tonalite-Migmatite
Complex of the Rottenstone Domain, which is
characterized by a greater proportion of calc-alkaline
plutonic rocks (Crowe Island Complex) and is
interpreted as the plutonic root of the La Ronge arc
(Corrigan et al., 1998a; 1999). Also to the north, and
structurally above the volcanic rocks of the Central
Metavolcanic Belt, are two distinct sedimentary
assemblages: the Milton Island assemblage, consisting
of graphitic metaturbidites interpreted as an inter-arc
basin co-cval with the Central Metavolcanic Belt
(Corrigan et al., 1997); and the Park Island
I
2
assemblage, consisting ofpolymictic conglomerate
grading stratigraphically upwards into magnetitebearing arkose and psammite. The Park lsland
assemblage is interpreted to have been deposited in a
foreland basin on the southern margin of the Hearne
craton (Corrigan et al., 1998a, 1999).
2. Field Relationships in Study Areas
The two areas chosen for study (Figure 1) include two
splays of the Central Metavolcanic Belt: the Reed Lake
and Lawrence Point volcanic belts, described by
Maxeiner ( 1997, 1998, this volume) and Corrigan et al.
{I 997, 1998b), and a supracrustal assemblage that
includes volcanic and sedimentary rock, as well as
oxide and silicate facies banded iron formation on
Laxdal and Doucet islands (Corrigan et al. , I 998a,
1999). Some geological and mineralogical
characteristics of the Reed Lake and Lawrence Point
volcanic belts are consistent with those attributed to
alteration zones associated with ancient volcanogenic
massive sulphide deposits (e.g. Froese, 1997; Dobbe,
1994), and banded iron fonnation within the Laxdal
and Doucet islands area might represent the more distal
component of an ancient hydrothermal system.
a) Reed Lake and Lawrence Point Volcanic
Belts
These rocks, mapped previously by Sibbald ( 1977),
Stauffer et al. (1979), Ashton (1979), Maxeiner (1997,
1998, this volume), and Corrigan et al. (I 997, 1998a),
and redefined by Maxeiner (this volume) fonn part of a
northeastern extension of the Central Metavolcanic
Belt (Figure 2). The Reed Lake and Lawrence Point
volcanic belts (RL VB and LPVB), separated in this
area by the 1858 ±2 Ma Butler Island Pluton (Corrigan,
1999, pers. comm.), are likely two splays of a larger,
thicker volcanic belt. Both belts consist of volcanic
rocks, altered volcanic rocks, and associated sediments.
A distinctive feature of both the RL VB and LPVB is
gamct-cordierite-orthoamphibole and cummingtonitegamet schists, previously studied in some detail by
Ashton ( 1979). These, as well as associated gossans,
might indicate that synvolcanic hydrothermal
alteration, a favourable process for the development of
volcanogenic massive sulphide deposits, has likely
Department of Geological Sciences, University of Saskatchewan, I 14 Science Place, Saskatoon, SK S7N 5E2.
Geological Survey of Canada, Continental Geosciencc Division, 615 13ooth St., Ottawa. ON KI A OE9.
Saskalchewan Geological Survey
159
BIP
Butler Island pluton
MIP Milton Island pluton
MLP McMillan Lake pluton
RIP
Reynolds Island pluton
@·
Biotite-magnetite leucogranite
· · .... Mclennan Group (arkose, polymictic
' ' conglomerate, calcareous a rkose)
""'D
'5
o.
. .-~
'!!
J} Hornblende-magnetite monzonite, quartz monzonite
ro
::e
~
' "..!-~· Diorite/quartz-diorite
ro
0
-X, ~
'( ·X··'
Park Island metasedimentary assemblage (arko se,
polymictic conglomerate , calcareous arkose, psammite)
1///)
Milton Island metasedimentary assemblage
' , , ., ·· (psammite, psa mmopelite, pel1te)
,
v\ Central Metavolcanic Belt
·, v
' Volcano-sedimentary assemblages
~
'
Crowe Island complex (diorit1c to granitic banded
,.,. · · orthogneiss
- - Outline of Reindeer Lake
Io krn
Figure I -Map displaying the location ofthe study areas on Reindeer Lake, as well as the main tectonic components within
the northwestern Reindeer Zone. Abbreviations: LRD, La Ronge Domain; GD, Glennie Domain; TMC, Tonalite-Migmatite
Complex; PLD, Peter Lake Domain; FFD, Flin Flon Domain; SID, South Indian Domain; and C-SBZ, Churchill-Superior
Boundary Zone (after Corrigan et al., 1998a; Lewry et aL, 1990; Ashton, 1999).
occurred in this environment (e.g. Ashton, 1979;
Maxeiner, 1998). Both belts are cut by felsic to
ultramafic intrusions.
Within the RL VB and LPVB, several distinct rock
units are recognized. These include mafic calc-silicate
rock, intermediate to mafic volcanics with intercalated
epiclastic rock, cummingtonite-garnet-bearing schist,
cordierite-anthophyllite schist, and intercalated
sedimentary rock.
Rocks of the mafic calc-silicate unit are fine grained,
and generally dark grey to black amphibolites that
generally consist of hornblende, plagioclase, and
diopside. Garnet is a major component where there are
concentrations of calc-silicate minerals (Figure 3).
Minor phases include quartz, cummingtonite, titanite,
apatite, and calcite. Concentrations of calc-silicate
minerals, in the form of bands and pods, consist of
diopside, plagioclase, and sometimes garnet. Locally
these resemble deformed pillow selvages (Figure 3).
Intermediate volcanic rocks are generally lighter in
color than the mafic calc-silicate rocks, and include
160
more readily identifiable volcanic features, such as
lapilli (Figure 4). They are generally light to medium
grey, and fine grained, with hornblende, plagioclase,
biotite, garnet, and quartz as major minerals and
cummingtonite occurring locally.
Cummingtonite±gamet-bearing rocks with pods of
cordierite-orthoamphibole schist are a significant unit
in both the RL VB and LPVB (Figure 5). These rocks
are light to medium grey, fine to locally coarse grained,
and are composed of cummingtonite, hornblende,
biotite, plagioclase, quartz, and commonly garnet, with
anthophyllite, gedrite, cordierite, sillimanite, staurolite,
titanite, ilmenite, magnetite, and calcite as minor
phases. The cummingtonite and garnet porphyroblasts
range in size up to 4 cm in length and 1 cm in
diameter, respectively, and are set in a felsic matrix.
The garnets are rimmed by fine-grained plagioclase.
Stromatic leucosomes composed of quartz and
plagioclase locally account for up to 5 percent of the
total rock. The cordierite-orthoamphibole rocks (Figure
5) found among the cummingtonite schists are light to
medium grey and fine to medium grained. Plagioclase,
orthoamphibole (anthophyllite and gedrite), biotite,
Summary of Investigations J 999. Volume 2
Legend
<::::::,.
'.;;;. Biotite-mognetit e leuc ogra nite
( : · \ Mclennon Group
@
Diorit e/quortz-diorite,
incl. Butler Island Pluto n {BI P)
·/ / / · Milton Island
metosedime ntory assembla ge
Central Metavolc anic BeJt
•
Colc -silico te :>:gornet-be oring
m ofic roc k
Intermediate rock
Reindeer Lake
Cord ierite :>: garnet
--- o rthoomphibole schist
Infe rred contacts
Figure 2 - Generalized geology map ofthe Mooney-Gawthrop islands (Reindeer Lake) area, showing the spatial relationships
between main units (after Corrigan et al., 1997); RLVB, Reed Lake volcanic belt; and LPVB, Lawrence Point volcanic belt.
quartz, cordierite, and garnet are the dominant
minerals, with sillimanite, staurolite, spinel, and iron
oxides as minor phases. There is approximately 5 to 10
percent leucosomal melt, with quartz, plagioclase, and
cordierite comprising the major phases. The wide
variety of metamorphic phases, as well as the
preservation of earlier phases (i.e. staurolite) makes
these rocks good candidates for the qualitative
determination of P-T conditions.
Locally minor amounts ofpsammopelitic rock are
found intercalated within the volcanic units. These are
commonly fine to medium grained, light to medium
brown, and consist primarily of feldspars, quartz,
biotite, and minor opaque phases. Locally, these rocks
contain iron sulphides and are rust weathering.
b) Supracrustal Rocks ofLaxdal and Doucet
Islands
Figure 3 - Majic calc-silicate rock of the Lawrence Point
volcanic belt, showing the calc-silicate pods within a mafic
hornblende±garnet-bearing matrix. Outcrop is located on
the north side o/Gawthrop Island, and the scale card is
9cm long.
Saskatchewan Geological Survey
On Laxdal and Doucet islands, north of Amiskit Island
on Reindeer Lake, the supracrustal rocks include mafic
to intermediate volcanic rock, banded iron formation,
interbedded sedimentary rock, as well as abundant
tonalitic to gabbroic intrusive rock (Corrigan et al.,
l 998a, 1999, this volume) (Figure 6). Primary textures
in the volcanic rocks are rare, but locally tuffbreccias,
161
ash flows, and other pyroclastic rocks are recognized,
as well as possible relict pillows within the mafic
volcanic rock. Banded iron formation, found as
discrete layers on both islands, consists of silicate- and
oxide-facies varieties. The overall association of mafic
rocks and banded iron formation suggests subaqueous
volcanism.
At the structural base of the supracrustal rocks found
on both Laxdal and Doucet islands, in indeterminate
contact with the "grey gneiss" associated with the
Crowe Island Complex described below, are a series of
calc-silicate-bearing mafic volcanic and psammitic to
psammopelitic rocks overlain by silicate facies banded
iron formation (Figure 7). The calc-silicate-bearing
mafic rocks are typically fine to medium grained, dark
green to black weathering, with a mineralogy
consisting of hornblende, plagioclase, quartz, and local
garnet, with calc-silicate pods consisting primarily of
diopside, plagioc\ase, and garnet. This mineral
assemblage is similar to that seen within the mafic
calc-silicate rocks of the LPVB. The silicate-oxide
facies banded iron formation is medium to coarse
grained, and consists of quartz, grunerite, garnet,
magnetite, ilmenite, and plagioclase.
On the north edges of Laxdal and Doucet islands,
sillimanite-bearing psammitic to pelitic rocks are
interbedded with and overlie the BIF and mafic calcsilicate rocks (Figure 8). These rocks are fine to
medium grained, well foliated, and locally contain
sillimanite knots oriented parallel to F2 axial planes.
They also contain significant amounts ofbiotite,
potassium feldspar, and quartz, with zircon and
monazite as minor phases.
Figure 4 - Three to 4 cm long felsic to intermediate lapilli
set in a fine grained intermediate volcanic matrix,found
on a small island northwest of Wapus Island. Scale card is
9 cm long.
Figure 5 - Cordierite-orthoamphibole schist from the east
edge of Mooney Island, showing long radiating
porphyroblasts ofacicular orthoamphibole and a weak
crenulation cleavage formed during D1 • Scale card is 9 cm
long.
162
Overlying the volcanic and intercalated sedimentary
rocks of the Central Metavolcanic Belt are clast- to
matrix-supported conglomerates interpreted as the
basal unit of the Park Island assemblage (Corrigan et
al, I 998a, Figure 10). The character of the
conglomerates vary. On Laxdal Island, the
conglomerate is typically light in color, and is
dominated by intermediate volcaniclastic debris. Rare
clasts include banded oxide facies iron formation and
quartz. All clasts are generally sub-angular in shape
and range in size up to 20 cm in length. The matrix of
these rocks is typically light to medium grey in color,
fine to medium grained, with a mineral assemblage
consisting of hornblende, biotite, plagioclase, quartz,
and magnetite, and the rock is poorly to moderately
foliated. On Doucet Island, both matrix and clasts of
the conglomerate are more mafic in character,
primarily due to an increased magnetite component.
Clasts of banded oxide facies iron formation are more
abundant and those of volcaniclastic debris less so. The
occurrence of conglomerate found on Doucet Island is
distinct from that seen on Laxdal Island, but they are
interpreted as the same unit due to their structural
location and generally consistent composition.
Intruding and obscuring the contacts and relationships
between most of the above described units are late,
medium- to coarse-grained, foliated tonalitic sheets and
later undeformed pegmatite dykes. The interpretation
of the conglomerates as marking the base of the Park
Island assemblage, as well as possible Bouma
sequences within the pelites intercalated with the
Summary ofinvestigations 1999, Volume 2
56'56'
N
t
Reindeer Lake
Le g end
®
Pork Island a ssemblage
·" ••
Pluton~ Rocks
- Unconformity - - Milto n Island assemblage
Crowe l~and Compex
character. Partial melting in some
areas has resulted in the
production of a diatexite, with
only biotite schlieren remaining
of the original rock. Locally,
partial assimilation of earlier
gabbroic to granodioritic rock has
resulted in compositional and
textural variations of the " grey
gneiss". This unit is also cut by a
medium- to coarse-grained,
foliated tonalite and later
pegmatites. Contacts with
surrounding assemblages are not
exposed, so direct relationships
may only be inferred.
3. Metamorphic
Relationships
Three phases of deformation have
been delineated within the rocks
of the RLVB, LPBV, and Laxdal
Banded Iron Fo rmatio n
and Doucet islands (Stauffer et
Psamm,tic to psammopelitic roc k
al., 1979; Maxeiner, 1996, 1997,
Interred
l km
199 8; Corrigan et al. , 1997,
Contac ts
1998a, I 998b, 1999). Mineral and
textural characteristics related to
the D 1 event are restricted to very
Figure 6 - Map ofthe Laxdal and Doucet islands area, showing the relationships
fine-grained fabrics and textures,
between the volcanogenic, sedimentary, and plutonic rocks (after Corrigan et al.,
such as biotite grains, the long
1998a, this volume).
axes of which parallel S0 • These
characteristics are commonly
volcanics, suggests that the rocks on these islands
overprinted by D2 textures. The D2 event is
young towards the north.
contemporaneous with the peak rnetamorphic grade,
and coincides with the growth of amphibolite grade
To the south on both islands, the mafic calc-silicate
metamorphic minerals, including amphiboles, garnet,
rocks are in contact with a "grey gneiss" of uncertain
and recrystallized biotite. Regional-scale D2 structural
origin, previously interpreted as an orthogneiss
features include south-verging reclined to recumbent
correlated with the Crowe Island Complex of Corrigan
et al. ( I 998a, 1999). In general, this rock is medium to
coarse grained, composed primarily of quartz,
potassium feldspar, biotite, and plagioclase, and is
highly strained, resulting in a straight gneissic
•-
including gre y gnciss'
CalC-siricat e-beanng rno ric rock
Figure 7 - Majic calc-silicate rock and silicatefacies
banded iron formation, with lens cap for scale. Outcrop is
located on the northeast edge of Laxdal Island, with the
top of the photograph/acing west.
Saskatchewan Geological Survey
Figure 8 - Matrix supported conglomerate, consisting of
tectonically flattened angular clasts of intermediate
volcanic composition, set in an intermediate matrix,found
structurally overlying the maflc calc-silicate and
sedimentary rock to the south. C/asts are elongate parallel
to SJ foliation, as well as F 2 fold a.xes, and have been
refolded by F 3 folds. Outcrop located within a small bay on
the north edge of Laxdal Island. Hammer for scale.
/63
folds and south verging thrust faults (Corrigan et al.,
l 998a, 1999). The 0 3 event is characterized by northtrending open upright F 3 folds, and greenschist facies
metamorphism, possibly related to uplift. The M 1
metamorphic event is interpreted to have occurred over
both 0 1 and 0 2 events, but the greenschist facies
metamorphism related to D 3 uplift is interpreted as a
separate metamorphic event (M 2).
The lithotectonic assemblages within the RL VB,
LPVB, and the Laxdal and Doucet islands areas
include variably altered volcanic and sedimentary rock.
The cordierite-anthophyllite assemblage of the RL VB
provides the best source of peak metamorphic P-T
information for that region, while the petites ofLaxdal
Island provide the best assemblage for delineating the
P-T conditions for that area. The combination of the PT information from both areas allows for the constraint
of overall P-T conditions in the southern Reindeer
Lake area. The mineral assemblages associated with
each respective rock type are summarized in Table 1.
The reaction space outlined by the cordieriteorthoamphibole schists on Figure 9 is the result of
several observations. First, the occurrence of
sillimanite and anthophyllite as inclusions within
cordierite grains (Figure 10) suggests that they predate
the growth of these particular cordierite grains, but also
sheds light on the possible path these rocks followed in
order to reach this point. The first occurrence of
aluminosilicate is represented by 1 on Figure 9, where
it is bracketed at a lower temperature by the reactions
St+Crd----)Oa+As and/or St----)Crd+Alm+As. The lack of
relict cordierite or garnet preserved within
anthophyllite or sillimanite suggests that any early
cordierite or garnet were entirely consumed by the
prograde reaction Crd+Alm----)Oa+As. However,
staurolite inclusions within cordierite observed by
Ashton (1979) within these rocks may represent a relict
of the earlier St----)Crd+Alm+As reaction.
Again due to the inclusion of sillimanite and
anthophyllite within cordierite, these rocks are
interpreted to have undergone decompression, passing
back over the Oa+As----)Crd+Alm reaction curve (2 on
Figure 9). The lack of orthopyroxene within these
rocks allows for the upper temperature of these rocks
to be constrained by the reaction Cum+Alm----)Oa+Opx.
Lower pressure conditions are constrained by the
Oa+Alm----)Crd+Cum reaction curve, as no
cummingtonite was observed. This is a tentative lower
limit, as full mineralogical analysis of the amphiboles
has not been completed. Coexisting gedrite and
anthophyllite have, however, been observed within
these rocks, and likely represent conditions marked by
3 on Figure 9. This occurrence is interpreted to
represent a part of the retrograde path, as it plots well
away from the "peak" conditions.
The pelitic schists of the Laxdal and Doucet region are
the most useful indicators of P-T condition for that
area, and the resultant P-T space is outlined on Figure
9. The assemblage sillimanite+potassium feldspar+
biotite+plagioclase+quartz is typical for the upper
amphibolite facies. The reaction muscovite+quartz----)
sillimanite+potassium feldspar and the presence of
quartzofeldspathic leucosomes within these and the
surrounding rocks help delineate the lower temperature
conditions of these rocks. As neither cordierite nor
orthopyroxene have been observed, the upper limit of
temperature is constrained by the reactions
Bt+As----)Crd+Alm+Ksp and Bt+A]m----)Crd+Opx+Ksp.
Satisfactory limits on pressure are not as well defined
by this assemblage, but the lower limits are defined by
the conversion of the Qtz+Pl+Ksp+H20----)melt and the
Bt+As----)Crd+Alm+Ksp reaction curves. Upper limits
on pressure are defined by the lack of kyanite within
this assemblage.
The two areas represented by the two metamorphic
assemblages are separated by approximately 30 km
distance, but there are no major structural boundaries
between the units, allowing for their combined use in
the determination of peak P-T conditions for this
region. The combination of the stable reaction
assemblages exhibited by these two rock types is
outlined by the fully shaded area on Figure 9. The
conditions represented by this area constrain P-T
conditions for the supracrustal rocks of the area at
approximately 680° to 710°C and 4.8 to 6.5 kbar.
These conditions agree with P-T conditions outlined by
Ashton ( 1979) for the Mooney Island area.
4. Summary
The RL VB and LPVB, and the Laxdal and Doucet
islands area are interpreted to form part of the La
Ronge Domain in the southern Reindeer Lake area
(Maxeiner, 1997, 1998;Corriganeta/., 1997, 1998a,
l 998b, this volume). These areas are predominantly
underlain by volcanic and intercalated sedimentary
rock as well as compositionally variable intrusive rock.
Some rocks of the area show evidence of
premetamorphic seawater and hydrothermal alteration,
represented by cummingtonite-gamet and cordieriteanthophyllite assemblages. Peak metamorphic
Table 1 - Metamorphic mineral assemblages ofthe primary rock types used in P-T determinations. Major phases (>5 percent)
are indicated by a star (*), and minor phases (<5 percent) by a dash (-).
Rock Type
Cordierite+orthoamphibole-bearing schi st
Pelitcs
164
Anthophyll ite/
Gedrite
Cordieritc
Gamet
•
•
•
Sillimanite
Biotite
Pl agioclase
Potassium
Feldspar
•
•
•
•
Summary ofinvestigations I 999, Volume 2
8 -
KYANITE
--
6
·"!'
u
r J)
'('Cl
..c
5
~
Stauffer and Dave MacDougall,
have been extremely helpful. The
assistance of Blaine Novakowski
and Tom Bonli at the University
of Saskatchewan is also greatly
appreciated. The major funding
for this project comes from an
NSERC grant to K.M. Ansdell, as
well as logistical assistance from
both the Saskatchewan
Geological Survey and the
Geological Survey of Canada.
Reviews by Drs. Ken Ashton and
Gary Delaney greatly improved
the manuscript.
(I)
'-
:J
~
6. References
4 --
Ashton, K.E. (1979): The
geology of the Milton Island
map sheet ( east half),
Saskatchewan (64D-10E),
unpubl. M.Sc. Thesis, Univ.
Sask., 13 lp.
())
'-
a..
3
I
2 ANDALUSITE
I
I
1I
I
600
500
I
700
Temperature (°C)
pota ssic
nonpotass1c
nonca lcic
Mineral Abbreviatio ns
Al m -Almand ine
Ksp - Potassium Fe ldspar
As - Aluminosilicate
Ms - Muscovite
Bt - Biotite
Oa - Orthoamph1bo le
Chi - Ch lorite
Opx - Orthopyroxene
Pl - Plagioclase
Crd - Cordierite
Qtz - Quartz
Cum - Cummingtonite
Hbl - Ho rnblende
Figure 9 - P-T grid displaying the inferred P-T path ofthe discussed metamorphic
assemblages. Lightly shaded area represents the stable cordierite-orthoamphibole
assemblage, darkly shaded area represents the stable pelite assemblage, and the fully
shaded area represents the P-T area ofthe combined stable assemblages. Numbered
circles are referred to in the text. Locations ofreaction curves in P-T space after
Froese (1997 and ref therein) and Spear (1980, 1993).
temperatures appear to be constrained between 680°
and 710°C, with an upper pressure constraint of
approximately 4.8 to 6.5 kbar. Further geochemical
investigation of both the altered and unaltered volcanic
rocks will likely shed light on both the tectonic setting
of these assemblages, as well as the extent and type of
alteration present (e.g. via mass balance calculations,
Gresens, 1967).
5. Acknowledgments
The assistance and camaraderie ofT.G. MacHattie,
J. Chakungal, B. Lassen, L. Piper, S. Pehrsson,
T. Prokopiuk, R. Morelli, A.Williamson, and
C. Huebert, as well as discussions with Dr. Mel
Saskatchewan Geological Survey
-~~_(1999): A proposed
lithotectonic domainal reclassification of the
southeastern Reindeer Zone
in Saskatchewan; in
Summary of Investigations
1999, Volume 1,
Saskatchewan Geological
Survey, Sask. Energy Mines,
Misc. Rep. 99-4.1, p92- l 00.
Bickford, M.E., Macdonald, R.,
Lewry, J.F., and Pearson,
J.G. (1986): U-Pb zircon
geochronology project for
the Trans-Hudson Orogen:
Current sampling and recent
results; in Summary of
Investigations 1986,
Saskatchewan Geological
survey, Sask. Energy Mines,
Misc. Rep 86-4, plOl-107.
Corrigan, D., Bashforth, A., and Lucas, S. ( 1997):
Geology and structural evolution of the La RongeLynn Lake Belt in the Butler Island area (parts of
640-9 and -10), Reindeer Lake, Saskatchewan; in
Summary of Investigations 1997, Saskatchewan
Geological Survey, Sask. Energy Mines, Misc.
Rep. 97-4, p 18-30.
Corrigan, D., MacHattie, T.G. , Piper, L., Wright, D.,
Pehrsson, S., Lassen, B., and Chakungal, J.
(I 998a): La Ronge-Lynn Lake Bridge Project:
New mapping results from Deep Bay (parts of
64D-6 and -7) to North Porcupine Point (top of
64E-7 and -8), Reindeer Lake; in Summary of
Investigations 1998, Saskatchewan Geological
165
North America; Geol. Assoc. Can., Spec. Pap. 37,
p75-94.
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Summary of Investigations 1999, Volume 2