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Current Research (2019) Newfoundland and Labrador Department of Natural ResourcesGeological Survey, Report 19-1, pages 23-38
STRUCTURAL GEOLOGY OF A GOLD-BEARING QUARTZ VEIN SYSTEM,
WILDING LAKE REGION, CENTRAL NEWFOUNDLAND
I.W. Honsberger, W. Bleeker, H.A.I. Sandeman1 and D.T.W. Evans2
Geological Survey of Canada, Ottawa, ON, K1A 0E81Mineral Deposits Section
2Antler Gold Inc., Halifax, NS, B3J 3R7
ABSTRACT
The structurally controlled gold belt of central Newfoundland is emerging as a significant exploration jurisdiction inCanada. The gold district occurs within a northeast-trending structural corridor defined by crustal-scale faults extending fromsouthwestern to north-central Newfoundland. Silurian syn-orogenic polymict conglomerate (Rogerson Lake Conglomerate)characterizes the structural corridor. The presence of conglomerate reflects preservation of syn-orogenic upper crustal clas-tic sequences commonly associated with orogenic gold vein systems. The largest known gold resource along this corridoroccurs at Marathon Gold Corporation’s Valentine Lake property. Marathon’s most recent public news release on ValentineLake reports a measured and indicated gold resource of 2.69 Moz grading at 1.85 g/t and an inferred resource of 1.53 Mozgrading at 1.77 g/t. Recent exploration by Antler Gold Inc. on previously unexplored property in the Wilding Lake area, adja-cent to the northeast corner of the Valentine Lake property, exposed a system of gold-bearing quartz veins hosted by syn-oro-genic sedimentary rocks, felsic volcanic rocks and volcaniclastic rocks.
Detailed structural study of these gold-bearing zones on the Antler Gold Inc. property demonstrates that the main ~2-m-wide gold-bearing quartz vein, which extends for ~230 m along strike, cuts the conglomerate host and occurs within anoblique sinistral reverse shear zone that involved a component of north-northeast-directed thrusting. An early set of stacked,moderately dipping extensional quartz veins, consistent with sinistral reverse shear, emanate outward into the country rockfrom the main vein. Younger, more steeply dipping sets of extensional quartz veins cut the main vein and the earlier shallow-dipping vein set, and are consistent with at least transient phases of horizontal extension and dextral transpression.Chalcopyrite and secondary malachite occur locally in the early vein sets, but are more abundant overall within the later,steeper, extensional vein sets. A nearly conjugate set of steeply dipping extension fractures cut the main vein and the exten-sional vein sets. These fractures are typically filled with an assemblage of vuggy quartz–chalcopyrite–malachite ± tourmaline± pyrite ± hematite ± goethite ± bismuth–tellurium sulphide(s). Regional correlations suggest that the quartz vein system expe-rienced a progressive structural history during the Late Silurian and Early Devonian.
INTRODUCTION
Structurally controlled gold systems comprise the most
economically significant gold deposit type in Canada
(Hodgson, 1993). The largest gold district, the late Archean
Abitibi greenstone belt of the Canadian Shield (e.g., Poulson
et al., 2000; Robert, 2001; Bleeker, 2015) consists of miner-
alized vein systems disposed along polydeformed, crustal-
scale fault zones (Figure 1, inset; Hodgson, 1993; Kerrich
and Cassidy, 1994; Groves et al., 1998; Kerrich et al., 2000;
Goldfarb et al., 2001). In central Newfoundland, numerous
examples of epigenetic gold mineralization appear to be
associated spatially with crustal-scale fault zones that pre-
serve syn-orogenic clastic sedimentary rocks (Figure 1).
This first-order relationship suggests that gold-bearing
quartz veins throughout central Newfoundland are struc-
turally controlled (e.g., Evans, 1996), with broad similarities
to mineralization of the Abitibi greenstone belt (Figure 1;
Honsberger and Bleeker, 2018). However, the polymetallic
nature of many examples of gold mineralization in central
Newfoundland (e.g., Tallman, 1991; Tallman and Evans,
1994; Evans and Wilson, 1994; Dalton and Scott, 1995;
Evans, 1996; O’Driscoll and Wilton, 2005; Lake and
Wilton, 2006; Sandeman et al., 2013, 2017), may suggest
local intrusion-related hydrothermal fluid inputs (e.g.,Sillitoe and Thompson, 1998; Hart, 2007).
The slowly growing, largest proven gold resource in
Newfoundland (and among the top in Canada) is Marathon
Gold Corporation’s Valentine Lake gold property disposed
23
CURRENT RESEARCH, REPORT 19-1
along the Victoria Lake shear zone in central Newfoundland
(Figures 1 and 2A; Marathon Gold Corporation, press
release, October 30, 2018). Presently, this emerging gold
property is reporting a measured and indicated gold resource
of 2.69 Moz grading at 1.85 g/t and an inferred resource of
1.53 Moz grading at 1.77 g/t (Marathon Gold Corporation,
press release, October 30, 2018). These resources are based
on ore extracted from four open-pit resource shells, as well
as underground operations at the Leprechaun, Victory,
Sprite and Marathon deposits (Lycopodium Minerals
Canada Ltd., 2018). Structural examination of the
Leprechaun gold deposit of the Valentine Lake gold proper-
ty suggests that it is similar to the quartz–tourmaline vein
systems at Val-d’Or in the Abitibi (Marathon Gold
Corporation, Mountain Lake Resources Inc., press release,
November, 2012). The recent expansion of the Valentine
Lake gold property has stimulated renewed prospecting,
staking, exploration and study elsewhere along the major
encompassing structural corridor. The research reported
herein documents the lithological and structural setting of
recently discovered gold mineralization on a mineral explo-
ration industry property adjacent to the northeast corner of
the Valentine Lake property (Figure 2A, B). Antler Gold Inc.
has 100% interest in the claims on the property of the pres-
ent study. This is the first detailed non-industry geological
study of this prospective gold property.
GEOLOGICAL AND STRUCTURAL
SETTING OF EPIGENETIC GOLD
MINERALIZATION, CENTRAL
NEWFOUNDLAND
Numerous epigenetic gold deposits and showings occur
along crustal-scale faults within the Dunnage Zone of central
Newfoundland (Figure 1; Tuach et al., 1988; Evans, 1996,
1999). The eastern Dunnage Zone, (the Exploits Subzone), is
particularly well-endowed in gold deposits and showings
(Evans, 1996). The main gold-bearing structural belt in cen-
tral Newfoundland extends northeast from Cape Ray for
24
HUMBER ZONE
Neoproterozoic to Ordovician
Sedimentary, metasedimentary,
and volcanic rocks
Gneiss and granite
Meso-Neoproterozoic
DUNNAGE ZONE
Cambrian to Early Silurian
Ophiolitic rocks
Clastic and volcanic rocks
GANDER ZONE
Neoproterozoic to Ordovician
Metasedimentary rocks and
migmatite
AVALON ZONE
Neoproterozoic to Ordovician
Sedimentary, volcanic,
and intrusive rocks
INTRUSIVE ROCKS
Silurian to Carboniferous
Granitoids
Mafic Intrusions
Cambrian to Ordovician
Granitoids
Major Fault Zone
Gold deposit (Abitibi)
Gold mineralization
(Newfoundland)
OVERLAP SEQUENCES
Devonian to Carboniferous
Sedimentary and
volcanic rocks
Late Ordovician to Devonian
Sedimentary rocks
BBL Baie Verte Line
RIL Red Indian Line
DBL Dog Bay Line
VLSZ Victoria Lake Shear Zone
CRF Cape Ray Fault Gold mine (Newfoundland) 100 km
100 km
VLSZ
DBL
Jackson’s Arm
Sop’s ArmHammerdown
Hope Brook
Stog’er Tight
Cape Ray
DF
HBF
RIL
BB
L
CF
CRF
RF G
RUB
Nugget Pond
Hand
Camp
Valentine
Lake
Figure 2A
Moosehead
Antler Gold,
Wilding LakeILFZ
DP
ZF
CBFZ
CL
ZF
CL
ZF
DP
ZF
DP
ZF
MRF
PT
Hollinger-McIntyre
Pamour
Timmins
West
Dome
KirklandLake KLM
T
Ka
pu
ska
sin
gS
tru
ctu
ral
Zo
ne
Gre
nv
i ll e
Fr o
nt
Ch
R-N
Horne
KerrAddison
Doyon
Malartic
BordenLake
Sigma- Lamaque
Casa
Berardi
Fogo Island
Figure 1. Comparison of Abitibi (left) and Newfoundland (right) geology and gold systems at the same regional scale. Thesame rock types are the same colours on both the Abitibi and Newfoundland maps; however, detailed explanation of geolog-ical zones and rock units is for Newfoundland. The area outlined in black is enlarged in Figure 2A. Abitibi map modified afterPoulsen et al. (2000), Dubé and Gosselin (2007), and Bleeker (2015). Newfoundland map adapted after Colman-Sadd et al.
(1990), with gold occurrences from Evans (1996), O’Driscoll and Wilton (2005), and Sandeman et al. (2017). Abbreviations:CBFZ, Casa Berardi Fault Zone; CF, Cabot Fault; Ch, Chapleau; CLFZ, Cadillac-Larder Lake Fault Zone; DF, Dover Fault;DPFZ, Destor-Porcupine Fault Zone; GRUB, Gander River Ultrabasic Belt; HBF, Hermitage Bay Fault; KL, Kirkland Lake;M, Matheson; MRF, the Paleoproterozoic Matagami River Fault; PT, the Pipestone Thrust; R-N, Rouyn-Noranda; T, Timmins.
I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
25
Valentine Lake project
Antler Gold’s Wilding Lake project
Granitoid
Ma!c volcanic
Ma!c instrusive
Ophiolite
Devonian granitoid
Felsic to ma!c volcanicMigmatite
Metasedimentary
Granitoid
Volcanic
Metamorphic complex
Neoproterozoic
rocks
Cambrian to Ordovician rocks
Volcaniclastic
Ma!c intrusive
Silurian granitoid
Carboniferous clastic sediment
Granitoid
Late Ordovician to Carboniferous rocks
Turbidite
Rogerson Lake Conglomerate
Thrust fault
25 km
N
A
423 +3/-2 Ma
ca. 387-402 Ma
ca. 564 ± 2 Ma
ca. 565 +4/-3 Ma
386 Ma
467 ± 6 Ma
457 ± 6 Ma
ca. 465 Ma
468 +3.5/-3 Ma
464 ± 3 Ma
Valentine Lake
thrust fault
Valentine Lake pluton
Red Indian Lake
Red Indian Line
Victoria Lake
shear zone
Badger Group
Stony Lake
volcanics
Paradise Lake
monzonite
Wilding
Lake
Quinn
Lake
Rogerson
Lake
Raven Birch
Alder/Taz
Elm/Cedar Zone
49.3 g/t over 4.6 m
101.5 g/t over 0.5 m
3.19 g/t over 0.75 m
563 Ma
513 2 Ma±
2 km
N
A
Cambrian felsic volcanic
and volcaniclastic rocks
Ordovician felsic volcanic rocks
Katian shale
Silurian Rogerson Lake Conglomerate
with local arenite interbeds
Red Ochre Complex
Third Spot
1.51 g/t over 11.0 m
A’
Dogberry
Valentine Lake thrust fault
Fault
Gold showing
Gold showing/
trench
Bridge
Ma�c dyke
B
Figure 2. A) Generalized geological map of thegold-bearing structural corridor, centralNewfoundland. Thrust faults are traced in red.The large orange circle marks the Valentine Lakegold project and the large yellow circle marksAntler Gold’s Wilding Lake project. Map adapt-ed from van Staal et al. (2005), Rogers et al.
(2005) and Valverde-Vaquero et al. (2005). Agesfrom Dunning et al. (1990), Evans et al. (1990),Rogers et al. (2005) and Valverde-Vaquero et al.
(2006). Map legend is applicable to Figure 2B;B) Generalized geological map of the WildingLake region. A-A′ represents the trace of thecross-section illustrated in Figure 3. Map adapt-ed from Valverde-Vaquero et al. (2005). Agesfrom Evans et al. (1990).
CURRENT RESEARCH, REPORT 19-1
~400 km to Fogo Island (Figure 1), and is characterized by
crustal-scale fault zones that locally preserve polymict con-
glomerate. The gold-bearing fault zones, from southwest to
northeast, are the Cape Ray fault, Red Indian Line and
Victoria Lake shear zone, and Dog Bay Line (Figure 1).
Marathon Gold Corporation’s Valentine Lake gold property
occurs along the Victoria Lake shear zone (Valverde-Vaquero
and van Staal, 2001) just northeast of Victoria Lake, where-
as the Antler Gold Inc. property in the Wilding Lake region
occurs farther northeast along the same structure (Figures 1
and 2A). Silurian Rogerson Lake Conglomerate occurs along
the major fault zone in both locations.
The geology of the gold-bearing corridor is character-
ized by accreted Neoproterozoic to Ordovician magmatic‒
sedimentary arc terranes of peri-Gondwanan affinity with
overlying Early Ordovician to Silurian sequences composed
of volcanic and sedimentary rocks (Williams, 1978;
Williams et al., 1988, 1993; Colman-Sadd et al., 1990;
Evans and Kean, 2002; O’Brien, 2003; Rogers et al., 2005,
2006; Valverde-Vaquero et al., 2005; van Staal et al., 2005).
The Valentine Lake pluton, a Neoproterozoic granitoid of
the Crippleback Intrusive Suite (Colman-Sadd et al., 1990;
Evans et al., 1990; van Staal et al., 2005) hosts gold miner-
alization at the Valentine Lake gold property (Figure 2A).
The gold resource at Valentine Lake occurs in the hanging
wall of the steeply northwest-dipping Valentine Lake thrust,
which places the Valentine Lake pluton over Rogerson Lake
Conglomerate (Marathon Gold Corporation, corporate pres-
entation, October 30, 2018). Rogerson Lake Conglomerate
is interpreted to represent the southwestern continuation of
the Silurian Botwood Group (Williams, 1972), which is
dominated farther northeast by red, green and grey-green
sandstones of the Wigwam Formation and magmatic rocks
of the Mount Peyton intrusive suite and Fogo Island
batholith (Colman-Sadd et al., 1990; O’Brien, 2003). An
Upper Ordovician to Devonian volcano-sedimentary
sequence containing polymict conglomerate occurs along
the gold-bearing Cape Ray fault (Dubé et al., 1996; van
Staal et al., 1996) in a structural position comparable to
Rogerson Lake Conglomerate.
Gold mineralization on Antler Gold’s property at
Wilding Lake occurs along the northeastern extension of the
Valentine Lake thrust, and is hosted within footwall rocks
composed of Rogerson Lake Conglomerate and inferred
Ordovician volcanic and volcaniclastic rocks (Figures 2B
and 3). Grey, muscovitic, medium-grained quartz arenite
beds interlayered with Rogerson Lake Conglomerate (Plate
1A) in the Wilding Lake region preserve local younging-
direction reversals (Plate 1B) consistent with tight upright
folding and a synclinal structure for the Silurian rocks and
underlying Ordovician rocks (Figure 3). The syncline is trun-
cated on the northwest by the northeastern extension of the
Valentine Lake thrust, which places Neoproterozoic volcanic
rocks and Cambrian to Ordovician arc rocks toward the
southeast over the Silurian‒Ordovician sequence (Figure 3).
The contact between Silurian Rogerson Lake Conglomerate
and the Ordovician volcanic and volcaniclastic rocks is not
exposed in this area; however, the absence of Late
Ordovician to Early Silurian Badger Group implies that the
contact is a deformed unconformity (Figure 3). The overall
structure suggests preservation of Silurian conglomerates in
a broad, partially truncated “footwall syncline” identical to
panels of syn-orogenic conglomerates in the Abitibi green-
stone belt (Bleeker, 2015). The overall synclinal structure
may also help explain local outcrops of conglomerate pre-
served above Ordovician volcanic and volcaniclastic rocks
south of the gold showings (Figures 2B and 3).
In the Wilding Lake area, gold mineralization is hosted
by Silurian Rogerson Lake Conglomerate as well as
Ordovician volcanic and volcaniclastic rocks. The Red
Ochre Complex, a gold-bearing feldspar porphyry unit,
occurs within the inferred Ordovician volcanic-volcaniclas-
tic sequence (Figure 3 and Plate 1C), whereas smaller gold
showings (e.g., Birch Zone) occur near the Rogerson Lake
Conglomerate‒Ordovician felsic volcanic contact (Figure 3
and Plate 1D). In Rogerson Lake Conglomerate, gold min-
eralization is associated with laterally extensive quartz veins
(e.g., Elm Zone and Alder Zone) that dip moderately to the
southeast and preserve structural evidence for oblique sinis-
tral shear. Gold is associated with quartz, chalcopyrite,
Bi–Te sulphides, tourmaline, and secondary malachite.
EXPLORATION HISTORY OF
THE VALENTINE LAKE
AND WILDING LAKE AREAS
From the early 1960s to 1998, base-metal exploration in
the Valentine Lake region by Asarco, Hudson Bay Oil and
Gas, Abitibi-Price, BP Canada, and Noranda led to the dis-
covery of quartz veins containing gold (Marathon Gold
Corporation, Mountain Lake Resources Inc., press release,
November, 2012). In 2006, InnovExplo studied the structure
of the Valentine Lake gold system and compared it to
quartz‒tourmaline gold deposits at Val-d’Or in the Abitibi
(Marathon Gold Corporation, Mountain Lake Resources
Inc., press release, November, 2012). The main deposit,
Marathon, presently defines a resource pit shell down to a
depth of ~1 km, with 1.9 Moz of measured and indicated
gold at 1.765 g/t (Marathon Gold Corporation, corporate
presentation, October 30, 2018).
Gold exploration in the Wilding Lake area began in
2015, when prospectors discovered visible gold in quartz
boulders along new logging roads. Prospecting and soil
sampling by Altius Resources in the summer of 2016 led to
26
I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
the discovery of additional quartz–tourmaline boulders with
visible gold. In September 2016, Antler Gold Inc. (Antler)
optioned the Wilding Lake property from Altius Resources.
Subsequent trenching between September 2016 and
November 2016 by Antler Gold Inc. exposed five new gold
showings, including Alder, Taz, Elm, Cedar and Dogberry,
all hosted in Rogerson Lake Conglomerate (Antler Gold
Inc., press release, August 30, 2017). Prospecting also iden-
tified three additional showings near the boundary with
inferred Ordovician felsic volcanic rocks (Birch, Third Spot
and Bridge). In 2017, Antler discovered the Red Ochre
Complex within the volcaniclastic rock-dominated terrane
south of the contact with Rogerson Lake Conglomerate, and
they exposed and defined more completely the other recent-
ly discovered gold-bearing zones. A first phase of channel
sampling and drilling was completed by Antler in 2017,
including three drillholes in the Alder Zone and 13 drillholes
in the Elm Zone (Antler Gold Inc., press release, December
13, 2017). Gold values of 19.2 g/t over 0.9 m and 49.92 g/t
over 0.98 m were reported for the Alder and Elm zones,
respectively, with local gold values of 101.5 g/t at Elm
(Antler Gold Inc., press release, January 24, 2017).
STRUCTURAL GEOLOGY, ELM ZONE,
WILDING LAKE PROPERTY
The gold-bearing quartz vein system of the Elm Zone
(Figures 4 and 5 and Plate 2) is the focus of this report
because it is the most extensive vein system known on the
property1, and has yielded the highest gold assays. Gold val-
ues within the main quartz vein are higher in the southwest-
ern trench (Figure 4B) than in the northeastern trench
(Figure 4A). The main quartz vein cuts Rogerson Lake
Conglomerate (Plate 2A), dips moderately (35–65°) to the
27
Plate 1. Field photographs. A) Interlayered polymict conglomerate and sandstone, Rogerson Lake Conglomerate; B) Basalscour in sandstone, Rogerson Lake Conglomerate; C) View toward the west of a gold-bearing quartz vein in feldspar por-phyry, Red Ochre Complex; D) Altered conglomerate, Birch Zone.
1Trenches were studied in the field prior to being backfilled in Fall 2018.
CURRENT RESEARCH, REPORT 19-1
28
NW SE
Deformation zone
Neoproterozoic volcanic
rocks
Cambrian volcanic rocks
Cambrian granitoid
Ordovician
volcaniclastic ±
magmatic rocks
Ordovician
volcanic rocks
Silurian Rogerson Lake
Conglomerate300 m 300 m
1 km ~5x Vertical Exaggeration
Elm
Birch
Red Ochre
Alder
A A’
Unconformity
Valentine Lake
thrust fault
surface
Figure 3. Interpreted cross-sectional view along A-A′. Locations of mineralized zones are indicatedwith yellow circles (Red Ochre Complex and Birch Zone) and short orange lines (Elm Zone and AlderZone). White circle marks the location of field photographs of Rogerson Lake Conglomerate shownin Figures 4A and 4B.
Figure 4A. (Figure on page 29) (Top) Orthorectified drone image of the northeastern portion of the Elm trench. The mainquartz vein (white lineament) cuts deformed and altered Rogerson Lake Conglomerate. Short black lines are the channel sam-ples traced on accompanying geological maps. Outlined areas are enlarged as geological maps in the lower portion of fig-ure. (Bottom) Geological maps of the northeastern portion of the Elm trench. The smaller map area covers the northeastern-most portion of the drone image, whereas the larger map area covers the southwestern portion. Foliations (grey lines), exten-sion veins (green lines), and fractures (purple lines) are superimposed. Different line thicknesses represent schematically vary-ing thicknesses of veins and fractures.
I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
29
Figure 4A. Caption on page 28.
C
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cpy
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cpy
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25
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8422
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4452
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7645
5456
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4451
85 35
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4280
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3465
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6146 35
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65
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8432
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5.83 g/t over 1.1 m
3.5 g/t over 1.0 m
3.76 g/t over 1.08 m
8.2 g/t over 0.88 m
1.95 g/t over 0.81 m
Early extensional quartz vein
Late extension fracture, quartz common
Early foliation
Late extensional quartz vein
Late foliation
Intersection lineationF1 Axial plane, vertical
F1 Fold axis
F2 Axial plane, vertical
F2 Fold axis
Bedding
Extension fracture
Extensional quartz vein
SlickenlineThrust fault
Very late extension fracture
N
Channel sample, Au value indicated
Early folia!on
Late folia!on
CT Chalcopyrite, tourmaline occurences
L Laminations in main quartz vein
Main quartz vein
Strongly altered conglomerate
Moderately to weakly
altered conglomerate A
10 mvq-mal-tur
72
66
54
55
7940
28
05
35
56
56
35
62
28
35
74
37
28
4260
41
35
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35 73
33
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6260
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68 11
74
4646
35
4531
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3734
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6450
4867
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77
3233
33
66
5649
4612
85
45
10 m
10 m
2.9 g/t over 1 m
5.4 g/t over 1 m
Northeastern Elm Trench
Early foliation
Late foliation
CURRENT RESEARCH, REPORT 19-1
southeast (Figure 5A), is up to 2.5 m wide, and is exposed
for about 230 m along strike to the northeast (Figure 4). It is
composed of multiple generations of laminated and massive,
medium- to coarse-grained milky white quartz in its interior
and near the hanging-wall contact, but more laminated and
carbonate-altered vein material proximal to the footwall
contact. The latter is marked by a zone of strongly deformed
conglomerate, locally transformed into a fault breccia.
Disseminated chalcopyrite, secondary malachite, and dark
fibrous tourmaline occur sporadically in the main vein.
Preliminary X-ray diffraction and scanning electron micro-
scope (SEM) investigations also identified abundant Bi–Te
sulphides.
The host conglomerate is typically purple-grey, clast-
supported and polymict, containing angular and subangular
to subrounded clasts up to ~15 cm in diameter consisting of
felsic to intermediate plutonic and volcanic rocks, clastic
sedimentary rocks, and jasper. The conglomerate is strongly
altered proximal (≤4 m) to the main vein (Plate 2B) and rel-
atively unaltered elsewhere (Plate 2C). Light to dark-brown
colouration of conglomerate is likely a result of ankerite
30
Late folia on
Early folia on
C
CC
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56
65
64
61
62
80
78
46
50
44
42
33
54
64
70
72
28
68
76
76
85
88
56
76
72
70
68
50
64
72
75
60
60
60
67
64
55
02
26
17
79
77
54
62
60
77
64
77
54
74
29
24
81
52
60
56
93.1 g/t over 1.3 m25.5 g/t over 0.8 m
28.5 g/t over 0.6 m
15.25 g/t over 0.9 m
101.5 g/t over 0.5 m
23.97 g/t over 0.3 m
N
Early extensional quartz vein
Late extension fracture, quartz common
Late extensional quartz vein
Very late extension fracture
Main quartz vein
Strongly altered conglomerate
Moderately to weakly
altered conglomerate
Early foliation
Late foliation
Intersection lineation
Bedding
Extension fracture
Extensional quartz vein
Thrust fault
F1 Axial plane, vertical
F1 Fold axis
F2 Axial plane, vertical
F2 Fold axis
Slickenline
Channel sample, Au value indicated
CT Chalcopyrite, tourmaline occurencesL Laminations in
main quartz vein
B
Southwestern Elm Trench
Early foliation
Late foliation
Figure 4B. (Top) Drone image of the southwestern portion of the Elm trench showing the continuation of the main quartz vein(white lineament). (Bottom) Geological map of the southwestern portion of the Elm trench. Map legend and symbols the sameas in (A).
I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
31
Figure 5. Lower hemisphere equal-area projections of relevant structures throughout the Elm Zone. A) Great circles showingattitudes of main quartz vein. Red circles show attitudes of slip lineations on main quartz vein, which are consistent withoblique thrusting; B) Poles to early foliation (Sn) and late foliation (Sn+1) in the hanging wall and footwall of the main quartzvein. Poles to bedding and the main quartz vein are plotted for reference. Representative attitude of axial plane and fold axisfor reclined folds are shown respectively as a great circle and pole; C) Great circles showing attitudes of early (V1) and late(V2) extensional quartz vein sets. The late vein set is richer in chalcopyrite, tourmaline, and secondary malachite; D) Greatcircles showing attitudes of conjugate extension fracture sets and, as well, a nearby mafic dyke. The attitude of the mafic dyke(black line) is subparallel to the northwest-dipping fracture set (bold purple lines), which is rich in vuggy quartz, chalcopy-rite, and secondary malachite, goethite and bismuth–tellurium sulphide(s).
Main Quartz Vein
Slip lineation
Thrust motion
D
U
D Downthrown block, Footwall
U Upthrown block, Hanging Wall
Fault zone
Extension Fractures
Mafic dyke
quartz-chalcopyrite
Main veinSn+1, Hanging Wall
Sn+1, Footwall
Sn, Hanging WallSn, Footwall
BeddingFold axis of reclined fold
Pole to axial plane
of reclined fold
Axial plane of
reclined fold
A B
C D
chalcopyrite-tourmaline-malachite
Late vein
Early vein
(V2)
(V1)
Extensional Quartz
Vein Sets
CURRENT RESEARCH, REPORT 19-1
32
Plate 2. Field photographs, Elm Zone. A) View toward the northeast of the main quartz vein cutting deformed Rogerson LakeConglomerate; B) Strongly altered conglomerate with quartz veinlets; C) Moderately to weakly altered conglomerate dis-playing local carbonate alteration of clasts; D) View toward the east of early, moderately dipping extensional quartz veins;E) View toward the south of late, steeply dipping extensional quartz vein with chalcopyrite and secondary malachite. Vein cutsdeformed conglomerate. Hand magnet above vein for scale; F) Vuggy quartz, tourmaline, chalcopyrite, and secondary mala-chite in late extension fracture. Red pen is pointing north.
I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
and/or siderite alteration, whereas fine-grained muscovite
(sericite) is likely responsible for the waxy luster in altered
conglomerate.
Primary bedding is locally preserved as sub-metre-scale
sandy layers in the conglomerate that typically strike subpar-
allel to foliation (Figure 5B). At least two generations of foli-
ations are preserved in the conglomerate. The older genera-
tion is well-preserved in the hanging wall of the main vein,
and typically strikes to the east-southeast and dips steeply
toward the south-southwest (Figure 5B). Deflection and shal-
lowing of this foliation into the main vein is consistent with
oblique sinistral shear and a component of thrusting toward
the north-northeast. The younger, crosscutting foliation
defines a spaced cleavage in the conglomerate that typically
dips shallowly to the northeast and southeast, and is locally
well-developed in the altered footwall of the main vein.
Where both foliations are present, the two form an intersec-
tion lineation that plunges shallowly to the southeast.
The deformed conglomerate is cut by the main vein,
which defines the main shear plane. Along the sheared con-
tact with hanging-wall conglomerate, the main vein displays
slickenlines plunging moderately toward the south-south-
west (Figure 5A). These linear features are also compatible
with oblique thrust motion toward the north-northeast
(Figure 5A). Stacked, deformed extensional quartz veins
(V1) consistent with sinistral shearing occur within strongly
altered conglomerate surrounding the main vein (Figure 4).
These extension veins dip moderately to shallowly to the
southeast and east-northeast (Plate 2D and Figure 5C), and
are locally folded into open to tight reclined folds that
plunge moderately to the southeast (Figure 5B). The axial
planes of such folds are subparallel to the main quartz vein
(Figure 5B), and the fold geometries are consistent with
drag folding during progressive oblique reverse shearing. A
late, steeply dipping set of extensional quartz veins (V2) cuts
the moderately dipping extensional vein set and also the
main quartz vein (Figures 4 and 5C and Plate 2E). This
younger vein set is richer in chalcopyrite, tourmaline, and
secondary malachite than the older vein set, with chalcopy-
rite filling vuggy spaces in the centre of the veins (Plate 2E).
Locally, another late set of steep extensional quartz veins
(V3) displaying asymmetry consistent with dextral motion
cuts the main quartz vein and early foliation. Steeply dip-
ping sets of nearly conjugate extension fractures cut the
main vein and both generations of extension veins (Figures
4 and 5D). The fracture set that dips moderately toward the
northwest (Plate 2F) is very tightly spaced in portions of the
main vein and usually contains vuggy quartz, chalcopyrite,
malachite ± tourmaline ± pyrite ± hematite ± goethite ± bis-
muth–tellurium sulphide(s), based on reconnaissance X-ray
diffraction and SEM studies. These particular fracture
planes form local intersection lineations on the main quartz
vein that are subparallel to slightly oblique to the displace-
ment vectors (slickenlines). A ~1.8-m-wide, carbonate-
altered mafic dyke that occurs ~200 m northwest of the Elm
Zone (Figure 2B) also displays a moderately northwest-dip-
ping orientation (Figure 5D). The youngest planar structures
observed in the Elm Zone are very late, weakly developed
fracture sets that parallel both the early foliation and lami-
nations in the main quartz vein.
KINEMATICS−ELM ZONE
The overall coherent geometry of the quartz vein sys-
tem and relatively consistent mineralogy of the different
vein sets is compatible with one progressive deformation
cycle. The conglomerate-hosted quartz vein system of the
Elm Zone defines an oblique sinistral contractional shear
zone that accommodated north to north-northeast-directed
shearing of the hanging wall relative to the footwall (Figure
6). Brittle overprint of earlier ductile shear structures sug-
gests that progressive deformation may have occurred in
the upper crust during exhumation of the conglomerate
across the brittle‒ductile transition, a depth of ~10 km
based on experimentally derived flow laws (e.g., Gleason
and Tullis, 1995).
The main gold-bearing quartz vein and associated
extensional structures cut sheared conglomerate, implying
that shearing was initiated prior to emplacement of the main
vein. Thickness variations in the main vein are compatible
with deposition of silica-rich fluids in semi-brittle dilata-
tional jogs that formed during sinistral, reverse shearing.
Folding of stacked extension veins (V1) where the main vein
is thinnest in the northeast of the trench supports progressive
compressional semi-ductile deformation. The late, brittle,
steep crosscutting vein set (V2) and late, shallow foliation
suggest rotation of the maximum principal stress (σ1) to sub-
vertical, potentially reflecting vertical shortening related to
structural collapse or a transient phase of syn-orogenic
extension. The local occurrences of late, steep veins with
dextral asymmetry (V3) may reflect a late episode of local-
ized transpression. Although the late sets of extension frac-
tures crosscut most veins, their geometries suggest that they
may have formed under a similar state of stress as the late
vein sets. The abundance of chalcopyrite, malachite, and
ankerite‒siderite in the extensional veins and fractures sug-
gests that Cu2+ and CO2, and likely Au, were mobilized mul-
tiple times during deformation of the main vein system.
GEOCHRONOLOGICAL IMPLICATIONS
Considering the Silurian tectonic evolution of the
Exploits Subzone (Dunning et al., 1990; Williams et al.,1993; O’Brien, 2003; van Staal et al., 2014), deformation in
the Elm Zone may have spanned Late Silurian to Early
33
CURRENT RESEARCH, REPORT 19-1
Devonian times. Regionally, deformed sedimentary rocks
and locally deformed magmatic rocks of the Botwood
Group disconformably overlie ca. 433 Ma and older sedi-
mentary rocks of the Badger Group, which were first
deformed during the earliest phase of Salinic deformation
(van der Pluijm et al., 1993; O’Brien, 2003). The
Badger‒Botwood Group unconformity is interpreted to rep-
resent a time gap of at least 7 m. y (433–426), and is inferred
to correspond to the main phase of Salinic deformation (van
Staal et al., 2014). On this basis, folding of Rogerson Lake
Conglomerate, the apparent stratigraphic base unit of the
Botwood Group at Wilding Lake soon after deposition may
have been initiated in the Ludlovian (late Salinic) by ca. 425
Ma, and progressed during emplacement of the Stony Lake
volcanic rocks (Figure 2A) at ca. 423 Ma (Dunning et al.,1990; McNicoll et al., 2008) and the granitoid rocks of the
Mount Peyton intrusive suite between 425 and 418 Ma
(Sandeman et al., 2017). Constraining the crystallization age
34
Early extension
vein
Cross-cutting
extension vein
Extension fracture
Early foliation
Late foliation
NNE
10 m
SSW
20 m20 m
No Vertical Exaggeration
Main quartz vein
Strongly altered conglomerate
Moderately to weakly
altered conglomerate
Cross-section view parallel to slip lineations on main vein
Oblique thrust motion
Surface
Figure 6. Structural cross-section interpretation of the main quartz vein of the Elm Zone, with structural data superimposed.Black arrow describes sense of oblique sinistral thrust motion. The vuggy quartz–chalcopyrite-rich extension fracture set(bold purple lines in Figure 5D) is not shown because these fracture planes are subparallel to the cross-sectional slice.
I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
of a presently undated, largely undeformed, locally brecciat-
ed monzonite body at Paradise Lake (Figure 2A) may help
to define a minimum age of Late Silurian–Early Devonian
deformation in central Newfoundland.
The oblique sinistral north-northeast-directed contrac-
tional shear component of deformation in the Elm Zone is
compatible with Late Silurian–Early Devonian oblique
sinistral transpression documented elsewhere along north-
east-trending shear zones within the central Newfoundland
gold district (e.g., O’Brien, 1993, 2003; Dubé et al., 1996).
Such movement along the Cape Ray fault zone (Figure 1)
occurred at ca. 415 Ma based on a metamorphic monazite
age (Dubé et al., 1996), whereas intrusive relationships
along the Bay d’Est and Cinq Cerf fault zones (Hope Brook
gold deposit, Figure 1) constrain such motion to ca. 420 Ma
(O’Brien et al., 1991). Northeast-trending shear zones in
central Newfoundland similar to the Elm Zone are interpret-
ed to have accommodated sinistral transpression during
early Acadian north‒south shortening (Currie and Piasecki,
1989; Hibbard, 1994). The onset of subsequent brittle over-
print, including late-stage subhorizontal extension, and
coeval vein formation in the Elm Zone may have roughly
coincided with deformation in Late Silurian–Early
Devonian sedimentary rocks near the Dog Bay Line
(415–410 Ma, McNicoll et al., 2006), with minor compo-
nents of dextral transpression potentially late Early
Devonian or younger in age (e.g., Currie and Piasecki, 1989;
Dubé et al., 1996). Considering the abundance of unaltered
and altered sulphide minerals in the late brittle vein and frac-
ture sets of the Elm Zone, the age of gold mineralization
may be Early Devonian or younger. This is compatible with
a preliminary 411 Ma age of hydrothermal rutile from a
gold-bearing extensional quartz vein at Valentine Lake
(Dunsworth and Walford, 2018).
CONCLUSIONS
The field data documented herein confirm that Antler
Gold Inc.’s Elm Zone mineralization and related veins rep-
resents a structurally controlled gold-bearing quartz vein
system that is likely an extension of the well-endowed
Valentine Lake structure to the southwest. However, where-
as mineralization at Valentine Lake occurs in the structural
hanging wall of the Valentine Lake thrust zone, mineraliza-
tion at Wilding Lake occurs in the structural footwall of the
thrust zone. Footwall gold mineralization in association with
syn-orogenic clastic sedimentary rocks bears close resem-
blance to the major gold-bearing structures of the Abitibi
greenstone belt (see Bleeker, 2015). Deeper drillholes into
Rogerson Lake Conglomerate on the Antler property will be
important for determining its full economic potential, as
rigid plutonic rocks, which are rheologically favourable for
gold-bearing fluid entrapment, have been observed in drill-
core to structurally underlie the conglomerate at Wilding
Lake (Antler Gold Inc., press release, December 13, 2017).
Future exploration and drilling in the Wilding Lake region
might target both hanging wall and footwall rocks, particu-
larly in rheologically competent, chemically reactive host
rocks, both at depth on site and farther northeast along the
extension of the Valentine Lake thrust.
ACKNOWLEDGMENTS
Ian Honsberger is conducting TGI supported post-doc-
toral research at GSC Ottawa. Thanks to Cees van Staal
(GSC Vancouver) for field guidance and for reviewing an
earlier draft of the manuscript. Time spent in the field with
Neil Rogers (GSC Ottawa) was helpful. A special thanks to
the Lakeview Inn for providing comfortable lodging.
Collaboration with the Geological Survey of Newfoundland
and Labrador and Antler Gold Inc. is gratefully acknowl-
edged. Critical reviews by John Hinchey and Jared Butler
improved the manuscript.
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