Current Research (2019) Newfoundland and Labrador Department of Natural Resources Geological 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 0E8 1Mineral 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 in Canada. The gold district occurs within a northeast-trending structural corridor defined by crustal-scale faults extending from southwestern 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 corridor occurs at Marathon Gold Corporation’s Valentine Lake property. Marathon’s most recent public news release on Valentine Lake reports 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. 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 an oblique 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 rock from 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 quartz veins throughout central Newfoundland are struc- turally controlled (e.g., Evans, 1996), with broad similarities Structurally controlled gold systems comprise the most to mineralization of the Abitibi greenstone belt (Figure 1; economically significant gold deposit type in Canada Honsberger and Bleeker, 2018). However, the polymetallic (Hodgson, 1993). The largest gold district, the late Archean nature of many examples of gold mineralization in central Abitibi greenstone belt of the Canadian Shield (e.g., Poulson Newfoundland (e.g., Tallman, 1991; Tallman and Evans, et al., 2000; Robert, 2001; Bleeker, 2015) consists of miner- 1994; Evans and Wilson, 1994; Dalton and Scott, 1995; alized vein systems disposed along polydeformed, crustal- Evans, 1996; O’Driscoll and Wilton, 2005; Lake and scale fault zones (Figure 1, inset; Hodgson, 1993; Kerrich Wilton, 2006; Sandeman et al., 2013, 2017), may suggest and Cassidy, 1994; Groves et al., 1998; Kerrich et al., 2000; local intrusion-related hydrothermal fluid inputs (e.g., Goldfarb et al., 2001). In central Newfoundland, numerous Sillitoe and Thompson, 1998; Hart, 2007). examples of epigenetic gold mineralization appear to be associated spatially with crustal-scale fault zones that pre- The slowly growing, largest proven gold resource in serve syn-orogenic clastic sedimentary rocks (Figure 1). Newfoundland (and among the top in Canada) is Marathon This first-order relationship suggests that gold-bearing Gold Corporation’s Valentine Lake gold property disposed
23 CURRENT RESEARCH, REPORT 19-1
HUMBER ZONE GANDER ZONE Neoproterozoic to Ordovician Neoproterozoic to Ordovician Sedimentary, metasedimentary, Metasedimentary rocks and and volcanic rocks migmatite Meso-Neoproterozoic AVALON ZONE Gneiss and granite Neoproterozoic to Ordovician
Casa Sedimentary, volcanic,
t
Berardi n
o BFZ r and intrusive rocks F DUNNAGE ZONE C
e
l
l
i
v Cambrian to Early Silurian
n
e
r G Clastic and volcanic rocks OVERLAP SEQUENCES F Sigma- Lamaque Devonian to Carboniferous CL Z Stog’er Tight Horne F Malartic DP Z Jackson’s Arm Ophiolitic rocks Sedimentary rocks R-N Kerr Doyon Addison Sop’s Arm BBL Nugget Pond PT Fogo Island Late Ordovician to Devonian Kirkland Hammerdown M Lake KL Sedimentary and Hollinger F DBL -McIntyre DP Z volcanic rocks T Pamour F M Dome CL Z RF Hand INTRUSIVE ROCKS Camp GRUB
e Timmins RF n
o West Antler Gold, Silurian to Carboniferous Z
Z
l
F
a
r L
I Wilding Lake u
t F
c Granitoids
u DP Z
r t
S RIL Moosehead
g
n i
s Mafic Intrusions
a
k
s u
p DF a
K Cambrian to Ordovician Figure 2A Ch Granitoids VLSZ Borden Lake 100 km Valentine CF Lake Hope Brook HBF
Cape Ray CRF Major Fault Zone BBL Baie Verte Line Gold deposit (Abitibi) RIL Red Indian Line DBL Dog Bay Line Gold mineralization VLSZ Victoria Lake Shear Zone (Newfoundland) CRF Cape Ray Fault Gold mine (Newfoundland) 100 km
Figure 1. Comparison of Abitibi (left) and Newfoundland (right) geology and gold systems at the same regional scale. The same 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 after Poulsen 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. along the Victoria Lake shear zone in central Newfoundland recently discovered gold mineralization on a mineral explo- (Figures 1 and 2A; Marathon Gold Corporation, press ration industry property adjacent to the northeast corner of release, October 30, 2018). Presently, this emerging gold the Valentine Lake property (Figure 2A, B). Antler Gold Inc. property is reporting a measured and indicated gold resource has 100% interest in the claims on the property of the pres- of 2.69 Moz grading at 1.85 g/t and an inferred resource of ent study. This is the first detailed non-industry geological 1.53 Moz grading at 1.77 g/t (Marathon Gold Corporation, study of this prospective gold property. press release, October 30, 2018). These resources are based on ore extracted from four open-pit resource shells, as well GEOLOGICAL AND STRUCTURAL as underground operations at the Leprechaun, Victory, SETTING OF EPIGENETIC GOLD Sprite and Marathon deposits (Lycopodium Minerals Canada Ltd., 2018). Structural examination of the MINERALIZATION, CENTRAL Leprechaun gold deposit of the Valentine Lake gold proper- NEWFOUNDLAND ty suggests that it is similar to the quartz–tourmaline vein systems at Val-d’Or in the Abitibi (Marathon Gold Numerous epigenetic gold deposits and showings occur Corporation, Mountain Lake Resources Inc., press release, along crustal-scale faults within the Dunnage Zone of central November, 2012). The recent expansion of the Valentine Newfoundland (Figure 1; Tuach et al., 1988; Evans, 1996, Lake gold property has stimulated renewed prospecting, 1999). The eastern Dunnage Zone, (the Exploits Subzone), is staking, exploration and study elsewhere along the major particularly well-endowed in gold deposits and showings encompassing structural corridor. The research reported (Evans, 1996). The main gold-bearing structural belt in cen- herein documents the lithological and structural setting of tral Newfoundland extends northeast from Cape Ray for
24 I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
ca. 565 +4/-3 Ma Badger Group
Paradise Lake monzonite Red Indian Lake Stony Lake N Valentine Lake pluton volcanics ca. 564 ± 2 Ma Red Indian Line 423 +3/-2 Ma ca. 465 Ma
386 Ma 25 km 464 ± 3 Ma 457 ± 6 Ma Thrust fault
Valentine Lake project
Antler Gold’s Wilding Lake project 468 +3.5/-3 Ma Valentine Lake Late Ordovician to Carboniferous rocks thrust fault Carboniferous clastic sediment ca. 387-402 Ma Devonian granitoid Cambrian to Ordovician rocks Victoria Lake Rogerson Lake Conglomerate Metamorphic complex shear zone Volcaniclastic Metasedimentary Silurian granitoid Neoproterozoic Granitoid rocks Migmatite Felsic to ma!c volcanic Volcanic Ma!c instrusive 467 ± 6 Ma Granitoid Ma!c intrusive Granitoid Ma!c volcanic Ophiolite Turbidite A
Figure 2. A) Generalized geological map of the gold-bearing structural corridor, central 513± 2 Ma Newfoundland. Thrust faults are traced in red. Quinn Lake The large orange circle marks the Valentine Lake A gold project and the large yellow circle marks Antler Gold’s Wilding Lake project. Map adapt- Rogerson Elm/Cedar Zone Lake 101.5 g/t over 0.5 m ed from van Staal et al. (2005), Rogers et al. Ma c dyke 563 Ma (2005) and Valverde-Vaquero et al. (2005). Ages Alder/Taz 49.3 g/t over 4.6 m from Dunning et al. (1990), Evans et al. (1990), Raven Birch Rogers et al. (2005) and Valverde-Vaquero et al. 3.19 g/t over 0.75 m A’ Red Ochre Complex (2006). Map legend is applicable to Figure 2B; 1.51 g/t over 11.0 m Dogberry Third Spot Bridge B) Generalized geological map of the Wilding Valentine Lake thrust fault Lake region. A-A′ represents the trace of the N cross-section illustrated in Figure 3. Map adapt- ed from Valverde-Vaquero et al. (2005). Ages from Evans et al. (1990). 2 km
Silurian Rogerson Lake Conglomerate Wilding with local arenite interbeds Lake Fault B Katian shale Gold showing Ordovician felsic volcanic rocks Cambrian felsic volcanic Gold showing/ and volcaniclastic rocks trench
25 CURRENT RESEARCH, REPORT 19-1
~400 km to Fogo Island (Figure 1), and is characterized by Valentine Lake thrust, which places Neoproterozoic volcanic crustal-scale fault zones that locally preserve polymict con- rocks and Cambrian to Ordovician arc rocks toward the glomerate. The gold-bearing fault zones, from southwest to southeast over the Silurian‒Ordovician sequence (Figure 3). northeast, are the Cape Ray fault, Red Indian Line and The contact between Silurian Rogerson Lake Conglomerate Victoria Lake shear zone, and Dog Bay Line (Figure 1). and the Ordovician volcanic and volcaniclastic rocks is not Marathon Gold Corporation’s Valentine Lake gold property exposed in this area; however, the absence of Late occurs along the Victoria Lake shear zone (Valverde-Vaquero Ordovician to Early Silurian Badger Group implies that the and van Staal, 2001) just northeast of Victoria Lake, where- contact is a deformed unconformity (Figure 3). The overall as the Antler Gold Inc. property in the Wilding Lake region structure suggests preservation of Silurian conglomerates in occurs farther northeast along the same structure (Figures 1 a broad, partially truncated “footwall syncline” identical to and 2A). Silurian Rogerson Lake Conglomerate occurs along panels of syn-orogenic conglomerates in the Abitibi green- the major fault zone in both locations. stone belt (Bleeker, 2015). The overall synclinal structure may also help explain local outcrops of conglomerate pre- The geology of the gold-bearing corridor is character- served above Ordovician volcanic and volcaniclastic rocks ized by accreted Neoproterozoic to Ordovician magmatic‒ south of the gold showings (Figures 2B and 3). sedimentary arc terranes of peri-Gondwanan affinity with overlying Early Ordovician to Silurian sequences composed In the Wilding Lake area, gold mineralization is hosted of volcanic and sedimentary rocks (Williams, 1978; by Silurian Rogerson Lake Conglomerate as well as Williams et al., 1988, 1993; Colman-Sadd et al., 1990; Ordovician volcanic and volcaniclastic rocks. The Red Evans and Kean, 2002; O’Brien, 2003; Rogers et al., 2005, Ochre Complex, a gold-bearing feldspar porphyry unit, 2006; Valverde-Vaquero et al., 2005; van Staal et al., 2005). occurs within the inferred Ordovician volcanic-volcaniclas- The Valentine Lake pluton, a Neoproterozoic granitoid of tic sequence (Figure 3 and Plate 1C), whereas smaller gold the Crippleback Intrusive Suite (Colman-Sadd et al., 1990; showings (e.g., Birch Zone) occur near the Rogerson Lake Evans et al., 1990; van Staal et al., 2005) hosts gold miner- Conglomerate‒Ordovician felsic volcanic contact (Figure 3 alization at the Valentine Lake gold property (Figure 2A). and Plate 1D). In Rogerson Lake Conglomerate, gold min- The gold resource at Valentine Lake occurs in the hanging eralization is associated with laterally extensive quartz veins wall of the steeply northwest-dipping Valentine Lake thrust, (e.g., Elm Zone and Alder Zone) that dip moderately to the which places the Valentine Lake pluton over Rogerson Lake southeast and preserve structural evidence for oblique sinis- Conglomerate (Marathon Gold Corporation, corporate pres- tral shear. Gold is associated with quartz, chalcopyrite, entation, October 30, 2018). Rogerson Lake Conglomerate Bi–Te sulphides, tourmaline, and secondary malachite. is interpreted to represent the southwestern continuation of the Silurian Botwood Group (Williams, 1972), which is EXPLORATION HISTORY OF dominated farther northeast by red, green and grey-green THE VALENTINE LAKE sandstones of the Wigwam Formation and magmatic rocks AND WILDING LAKE AREAS of the Mount Peyton intrusive suite and Fogo Island batholith (Colman-Sadd et al., 1990; O’Brien, 2003). An From the early 1960s to 1998, base-metal exploration in Upper Ordovician to Devonian volcano-sedimentary the Valentine Lake region by Asarco, Hudson Bay Oil and sequence containing polymict conglomerate occurs along Gas, Abitibi-Price, BP Canada, and Noranda led to the dis- the gold-bearing Cape Ray fault (Dubé et al., 1996; van covery of quartz veins containing gold (Marathon Gold Staal et al., 1996) in a structural position comparable to Corporation, Mountain Lake Resources Inc., press release, Rogerson Lake Conglomerate. November, 2012). In 2006, InnovExplo studied the structure of the Valentine Lake gold system and compared it to Gold mineralization on Antler Gold’s property at quartz‒tourmaline gold deposits at Val-d’Or in the Abitibi Wilding Lake occurs along the northeastern extension of the (Marathon Gold Corporation, Mountain Lake Resources Valentine Lake thrust, and is hosted within footwall rocks Inc., press release, November, 2012). The main deposit, composed of Rogerson Lake Conglomerate and inferred Marathon, presently defines a resource pit shell down to a Ordovician volcanic and volcaniclastic rocks (Figures 2B depth of ~1 km, with 1.9 Moz of measured and indicated and 3). Grey, muscovitic, medium-grained quartz arenite gold at 1.765 g/t (Marathon Gold Corporation, corporate beds interlayered with Rogerson Lake Conglomerate (Plate presentation, October 30, 2018). 1A) in the Wilding Lake region preserve local younging- direction reversals (Plate 1B) consistent with tight upright Gold exploration in the Wilding Lake area began in folding and a synclinal structure for the Silurian rocks and 2015, when prospectors discovered visible gold in quartz underlying Ordovician rocks (Figure 3). The syncline is trun- boulders along new logging roads. Prospecting and soil cated on the northwest by the northeastern extension of the 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
Plate 1. Field photographs. A) Interlayered polymict conglomerate and sandstone, Rogerson Lake Conglomerate; B) Basal scour 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. the discovery of additional quartz–tourmaline boulders with in the Elm Zone (Antler Gold Inc., press release, December visible gold. In September 2016, Antler Gold Inc. (Antler) 13, 2017). Gold values of 19.2 g/t over 0.9 m and 49.92 g/t optioned the Wilding Lake property from Altius Resources. over 0.98 m were reported for the Alder and Elm zones, Subsequent trenching between September 2016 and respectively, with local gold values of 101.5 g/t at Elm November 2016 by Antler Gold Inc. exposed five new gold (Antler Gold Inc., press release, January 24, 2017). showings, including Alder, Taz, Elm, Cedar and Dogberry, all hosted in Rogerson Lake Conglomerate (Antler Gold STRUCTURAL GEOLOGY, ELM ZONE, Inc., press release, August 30, 2017). Prospecting also iden- WILDING LAKE PROPERTY tified three additional showings near the boundary with inferred Ordovician felsic volcanic rocks (Birch, Third Spot The gold-bearing quartz vein system of the Elm Zone and Bridge). In 2017, Antler discovered the Red Ochre (Figures 4 and 5 and Plate 2) is the focus of this report Complex within the volcaniclastic rock-dominated terrane because it is the most extensive vein system known on the south of the contact with Rogerson Lake Conglomerate, and property1, and has yielded the highest gold assays. Gold val- they exposed and defined more completely the other recent- ues within the main quartz vein are higher in the southwest- ly discovered gold-bearing zones. A first phase of channel ern trench (Figure 4B) than in the northeastern trench sampling and drilling was completed by Antler in 2017, (Figure 4A). The main quartz vein cuts Rogerson Lake including three drillholes in the Alder Zone and 13 drillholes Conglomerate (Plate 2A), dips moderately (35–65°) to the
1Trenches were studied in the field prior to being backfilled in Fall 2018.
27 CURRENT RESEARCH, REPORT 19-1
Valentine Lake thrust fault NW SE surface A Elm A’
Alder Birch Red Ochre
Deformation zone
Unconformity Silurian Rogerson Lake Conglomerate 300 m 300 m Cambrian granitoid Ordovician volcanic rocks Cambrian volcanic rocks Ordovician Neoproterozoic volcanic volcaniclastic ± rocks magmatic rocks 1 km ~5x Vertical Exaggeration
Figure 3. Interpreted cross-sectional view along A-A′. Locations of mineralized zones are indicated with yellow circles (Red Ochre Complex and Birch Zone) and short orange lines (Elm Zone and Alder Zone). White circle marks the location of field photographs of Rogerson Lake Conglomerate shown in Figures 4A and 4B.
Figure 4A. (Figure on page 29) (Top) Orthorectified drone image of the northeastern portion of the Elm trench. The main quartz 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.
28 I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
Northeastern Elm Trench
2.9 g/t over 1 m
29
05 54 28 79 35 5.4 g/t over 1 m 40
56 55 56 66 34 35 35 41 28 72 60 42 62 74 62 37 35 73 35 28 25 46 46 56 27 22
28 60 62 16 74 35 47 31 45 56 28 34 06 84 50 68 11 36 84 58 45 64 65 71 77 45 32 33 35 32 88 67 67 48 37 12 33 21 34 63 46 37 68 10 m 86 37 49 85 56 76 vq-mal-tur
33
66
10 m
Thrust fault Slickenline 35 70 Extensional quartz vein F2 Fold axis 49 67 82 F2 Axial plane, vertical 25 Extension fracture 35 41 Bedding F1 Fold axis 55 Intersection lineation 45 29 F1 Axial plane, vertical 85 35 Late foliation 5.83 g/t over 1.1 m 30 83 26 44 80 51 42 58 66 33 72 70 Channel sample, Au value indicated 24 Early foliation 86 80 60 3.5 g/t over 1.0 m 42 64 C 80 74 CT Chalcopyrite, tourmaline occurences 52 65 34 68 L Laminations in main quartz vein C 18
52 27 41 55 05 30 08 13 37 67 67 24 65 83 78 49 78 41 84 C 40 T 61 Early folia!on 67 66 59 32 12 46 35 56 36 54 81 52 42 63 79 61 60 49 N 89 T 53 71 06 31 42 54 37 74 09 45 16 29 46 3.76 g/t over 1.08 m 37 49 09 23 37 70 34 04 73 75 76 49 C 88 80 15 61 71 L 73 70 35 34 76 56 L 84 52 42 55 52 71 86 60 76 37 44 54 84 46 44 51 C T 50 35 85 80 73 58 36 77 77 76 87 75 77 45 77 65 65 83 40 75 89 48 29 67 64 24 68 52 39 61 52 75 47 40 64 T 56 55 64 87 33 Late folia!on 55 82 C 79 64 8.2 g/t over 0.88 m 70 71 64 88 36 63 37 59 26 16 35 61 78 32 24 cpy 51 30 60 L 69 cpy 67 63 66 32 T 54 73 70 58 67 84 47 1.95 g/t over 0.81 m C CT C 83 79 45 76 76 C C 84 57 56 54 88 64 C L T 65 46 56 C 26 52 44 30 52 25 66 34 32 38 Late foliation 37 CT 67 76 40 22 44 28 22 40 21 58 C 59 Main quartz vein 44 C 69 Early foliation 63 62 62 74 70 C 46 64 79 89 51 74 84 38 30 85 Very late extension fracture 66 57 26 75 66 Strongly altered conglomerate 72 22 58 84 77 65 14 Late extension fracture, quartz common 34 34 54 43 68 26 41 76 Moderately to weakly Late extensional quartz vein 10 m altered conglomerate Early extensional quartz vein A
Figure 4A. Caption on page 28.
29 CURRENT RESEARCH, REPORT 19-1
Southwestern Elm Trench
Thrust fault Slickenline Extensional quartz vein F2 Fold axis Extension fracture F2 Axial plane, vertical Bedding Intersection lineation F1 Fold axis Late foliation F1 Axial plane, vertical Early foliation Channel sample, Au value indicated L Laminations in main quartz vein CT Chalcopyrite, tourmaline occurences
58 26 71 93.1 g/t over 1.3 m 76 25.5 g/t over 0.8 m 63 36 23 77 74 73 89 59 66 42 26 101.5 g/t over 0.5 m 66 58 73 54 C 72 88 60 74 59 70 73 C 50 C 80 68 56 72 56 88 26 66 51 71 76 58 53 68 C 68 T 40 84 50 61 15.25 g/t over 0.9 m C 80 74 56 60 83 55 54 58 CT 56 C 46 55 68 58 55 52 36 50 74 60 56 60 81 40 35 70 71 38 58 N 28.5 g/t over 0.6 m 78 65 55 45 50 78 65 50 75 70 50 44 48 55 77 55 76 80 42 54 77 64 70 55 84 76 55 38 C 65 70 62 86 75 45 76 78 65 65 55 76 74 50 32 23.97 g/t over 0.3 m 48 74 48 62 77 29 66 60 46 57 56 76
65 46
64
62
56 55 65
Early folia on 64
52 74 72 61 50 64 66 78 Late foliation
60 66 C 63 Late folia on 60 60 Main quartz vein 64 Early foliation 68 C 51 76 76 72 44 Very late extension fracture 80 78 54 88 62 Strongly altered conglomerate C 81 42 46 Late extension fracture, quartz common 29 52 33 85
54 50 60 54 75 79 74 Late extensional quartz vein 64 Moderately to weakly 28 70 02 24 64 77 26 72 56 67 60 B C 55 altered conglomerate Early extensional quartz vein 17 77 64 62 C 77
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 same as in (A). southeast (Figure 5A), is up to 2.5 m wide, and is exposed scope (SEM) investigations also identified abundant Bi–Te for about 230 m along strike to the northeast (Figure 4). It is sulphides. composed of multiple generations of laminated and massive, medium- to coarse-grained milky white quartz in its interior The host conglomerate is typically purple-grey, clast- and near the hanging-wall contact, but more laminated and supported and polymict, containing angular and subangular carbonate-altered vein material proximal to the footwall to subrounded clasts up to ~15 cm in diameter consisting of contact. The latter is marked by a zone of strongly deformed felsic to intermediate plutonic and volcanic rocks, clastic conglomerate, locally transformed into a fault breccia. sedimentary rocks, and jasper. The conglomerate is strongly Disseminated chalcopyrite, secondary malachite, and dark altered proximal (≤4 m) to the main vein (Plate 2B) and rel- fibrous tourmaline occur sporadically in the main vein. atively unaltered elsewhere (Plate 2C). Light to dark-brown Preliminary X-ray diffraction and scanning electron micro- colouration of conglomerate is likely a result of ankerite
30 I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS
A B Main Quartz Vein
Slip lineation
Thrust motion
D Downthrown block, Footwall
U Upthrown block, Hanging Wall
D Axial plane of reclined fold Fault zone
Main vein U Sn+1, Hanging Wall Sn+1, Footwall Sn, Hanging Wall Sn, Footwall Bedding Fold axis of reclined fold Pole to axial plane Extensional Quartz of reclined fold Vein Sets
quartz-chalcopyrite
chalcopyrite-tourmaline-malachite
Late vein (V2) Early vein (V ) 1 Mafic dyke
Extension Fractures C D
Figure 5. Lower hemisphere equal-area projections of relevant structures throughout the Elm Zone. A) Great circles showing attitudes of main quartz vein. Red circles show attitudes of slip lineations on main quartz vein, which are consistent with oblique thrusting; B) Poles to early foliation (Sn) and late foliation (Sn+1) in the hanging wall and footwall of the main quartz vein. Poles to bedding and the main quartz vein are plotted for reference. Representative attitude of axial plane and fold axis for 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) Great circles 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).
31 CURRENT RESEARCH, REPORT 19-1
Plate 2. Field photographs, Elm Zone. A) View toward the northeast of the main quartz vein cutting deformed Rogerson Lake Conglomerate; 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 cuts deformed 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.
32 I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS and/or siderite alteration, whereas fine-grained muscovite vein that are subparallel to slightly oblique to the displace- (sericite) is likely responsible for the waxy luster in altered ment vectors (slickenlines). A ~1.8-m-wide, carbonate- conglomerate. altered mafic dyke that occurs ~200 m northwest of the Elm Zone (Figure 2B) also displays a moderately northwest-dip- Primary bedding is locally preserved as sub-metre-scale ping orientation (Figure 5D). The youngest planar structures sandy layers in the conglomerate that typically strike subpar- observed in the Elm Zone are very late, weakly developed allel to foliation (Figure 5B). At least two generations of foli- fracture sets that parallel both the early foliation and lami- ations are preserved in the conglomerate. The older genera- nations in the main quartz vein. tion is well-preserved in the hanging wall of the main vein, and typically strikes to the east-southeast and dips steeply KINEMATICS−ELM ZONE toward the south-southwest (Figure 5B). Deflection and shal- lowing of this foliation into the main vein is consistent with The overall coherent geometry of the quartz vein sys- oblique sinistral shear and a component of thrusting toward tem and relatively consistent mineralogy of the different the north-northeast. The younger, crosscutting foliation vein sets is compatible with one progressive deformation defines a spaced cleavage in the conglomerate that typically cycle. The conglomerate-hosted quartz vein system of the dips shallowly to the northeast and southeast, and is locally Elm Zone defines an oblique sinistral contractional shear well-developed in the altered footwall of the main vein. zone that accommodated north to north-northeast-directed Where both foliations are present, the two form an intersec- shearing of the hanging wall relative to the footwall (Figure tion lineation that plunges shallowly to the southeast. 6). Brittle overprint of earlier ductile shear structures sug- gests that progressive deformation may have occurred in The deformed conglomerate is cut by the main vein, the upper crust during exhumation of the conglomerate which defines the main shear plane. Along the sheared con- across the brittle‒ductile transition, a depth of ~10 km tact with hanging-wall conglomerate, the main vein displays based on experimentally derived flow laws (e.g., Gleason slickenlines plunging moderately toward the south-south- and Tullis, 1995). west (Figure 5A). These linear features are also compatible with oblique thrust motion toward the north-northeast The main gold-bearing quartz vein and associated (Figure 5A). Stacked, deformed extensional quartz veins extensional structures cut sheared conglomerate, implying
(V1) consistent with sinistral shearing occur within strongly that shearing was initiated prior to emplacement of the main altered conglomerate surrounding the main vein (Figure 4). vein. Thickness variations in the main vein are compatible These extension veins dip moderately to shallowly to the with deposition of silica-rich fluids in semi-brittle dilata- southeast and east-northeast (Plate 2D and Figure 5C), and tional jogs that formed during sinistral, reverse shearing. are locally folded into open to tight reclined folds that Folding of stacked extension veins (V1) where the main vein plunge moderately to the southeast (Figure 5B). The axial is thinnest in the northeast of the trench supports progressive planes of such folds are subparallel to the main quartz vein compressional semi-ductile deformation. The late, brittle,
(Figure 5B), and the fold geometries are consistent with steep crosscutting vein set (V2) and late, shallow foliation drag folding during progressive oblique reverse shearing. A suggest rotation of the maximum principal stress (σ1) to sub- late, steeply dipping set of extensional quartz veins (V2) cuts vertical, potentially reflecting vertical shortening related to the moderately dipping extensional vein set and also the structural collapse or a transient phase of syn-orogenic main quartz vein (Figures 4 and 5C and Plate 2E). This extension. The local occurrences of late, steep veins with younger vein set is richer in chalcopyrite, tourmaline, and dextral asymmetry (V3) may reflect a late episode of local- secondary malachite than the older vein set, with chalcopy- ized transpression. Although the late sets of extension frac- rite filling vuggy spaces in the centre of the veins (Plate 2E). tures crosscut most veins, their geometries suggest that they Locally, another late set of steep extensional quartz veins may have formed under a similar state of stress as the late
(V3) displaying asymmetry consistent with dextral motion vein sets. The abundance of chalcopyrite, malachite, and cuts the main quartz vein and early foliation. Steeply dip- ankerite‒siderite in the extensional veins and fractures sug- 2+ ping sets of nearly conjugate extension fractures cut the gests that Cu and CO2, and likely Au, were mobilized mul- main vein and both generations of extension veins (Figures tiple times during deformation of the main vein system. 4 and 5D). The fracture set that dips moderately toward the northwest (Plate 2F) is very tightly spaced in portions of the GEOCHRONOLOGICAL IMPLICATIONS main vein and usually contains vuggy quartz, chalcopyrite, malachite ± tourmaline ± pyrite ± hematite ± goethite ± bis- Considering the Silurian tectonic evolution of the muth–tellurium sulphide(s), based on reconnaissance X-ray Exploits Subzone (Dunning et al., 1990; Williams et al., diffraction and SEM studies. These particular fracture 1993; O’Brien, 2003; van Staal et al., 2014), deformation in planes form local intersection lineations on the main quartz the Elm Zone may have spanned Late Silurian to Early
33 CURRENT RESEARCH, REPORT 19-1
NNE SSW Surface
Cross-section view parallel to slip lineations on main vein
20 m 20 m
Main quartz vein Strongly altered conglomerate Moderately to weakly altered conglomerate
Early extension Extension fracture vein Cross-cutting Late foliation extension vein Oblique thrust motion Early foliation
10 m No Vertical Exaggeration
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.
Devonian times. Regionally, deformed sedimentary rocks Staal et al., 2014). On this basis, folding of Rogerson Lake and locally deformed magmatic rocks of the Botwood Conglomerate, the apparent stratigraphic base unit of the Group disconformably overlie ca. 433 Ma and older sedi- Botwood Group at Wilding Lake soon after deposition may mentary rocks of the Badger Group, which were first have been initiated in the Ludlovian (late Salinic) by ca. 425 deformed during the earliest phase of Salinic deformation Ma, and progressed during emplacement of the Stony Lake (van der Pluijm et al., 1993; O’Brien, 2003). The volcanic rocks (Figure 2A) at ca. 423 Ma (Dunning et al., Badger‒Botwood Group unconformity is interpreted to rep- 1990; McNicoll et al., 2008) and the granitoid rocks of the resent a time gap of at least 7 m. y (433–426), and is inferred Mount Peyton intrusive suite between 425 and 418 Ma to correspond to the main phase of Salinic deformation (van (Sandeman et al., 2017). Constraining the crystallization age
34 I.W. HONSBERGER, W. BLEEKER, H.A.I. SANDEMAN AND D.T.W. EVANS of a presently undated, largely undeformed, locally brecciat- gold-bearing fluid entrapment, have been observed in drill- ed monzonite body at Paradise Lake (Figure 2A) may help core to structurally underlie the conglomerate at Wilding to define a minimum age of Late Silurian–Early Devonian Lake (Antler Gold Inc., press release, December 13, 2017). deformation in central Newfoundland. Future exploration and drilling in the Wilding Lake region might target both hanging wall and footwall rocks, particu- The oblique sinistral north-northeast-directed contrac- larly in rheologically competent, chemically reactive host tional shear component of deformation in the Elm Zone is rocks, both at depth on site and farther northeast along the compatible with Late Silurian–Early Devonian oblique extension of the Valentine Lake thrust. sinistral transpression documented elsewhere along north- east-trending shear zones within the central Newfoundland ACKNOWLEDGMENTS gold district (e.g., O’Brien, 1993, 2003; Dubé et al., 1996). Such movement along the Cape Ray fault zone (Figure 1) Ian Honsberger is conducting TGI supported post-doc- occurred at ca. 415 Ma based on a metamorphic monazite toral research at GSC Ottawa. Thanks to Cees van Staal age (Dubé et al., 1996), whereas intrusive relationships (GSC Vancouver) for field guidance and for reviewing an along the Bay d’Est and Cinq Cerf fault zones (Hope Brook earlier draft of the manuscript. Time spent in the field with gold deposit, Figure 1) constrain such motion to ca. 420 Ma Neil Rogers (GSC Ottawa) was helpful. A special thanks to (O’Brien et al., 1991). Northeast-trending shear zones in the Lakeview Inn for providing comfortable lodging. central Newfoundland similar to the Elm Zone are interpret- Collaboration with the Geological Survey of Newfoundland ed to have accommodated sinistral transpression during and Labrador and Antler Gold Inc. is gratefully acknowl- early Acadian north‒south shortening (Currie and Piasecki, edged. Critical reviews by John Hinchey and Jared Butler 1989; Hibbard, 1994). The onset of subsequent brittle over- improved the manuscript. print, including late-stage subhorizontal extension, and coeval vein formation in the Elm Zone may have roughly REFERENCES coincided with deformation in Late Silurian–Early Devonian sedimentary rocks near the Dog Bay Line Bleeker, W. (415–410 Ma, McNicoll et al., 2006), with minor compo- 2015: Synorogenic gold mineralization in granite- nents of dextral transpression potentially late Early greenstone terranes: The deep connection between Devonian or younger in age (e.g., Currie and Piasecki, 1989; extension, major faults, synorogenic clastic basins, Dubé et al., 1996). Considering the abundance of unaltered magmatism, thrust inversion, and long-term preserva- and altered sulphide minerals in the late brittle vein and frac- tion. In Targeted Geoscience Initiative 4: Contributions ture sets of the Elm Zone, the age of gold mineralization to the Understanding of Precambrian Lode Gold may be Early Devonian or younger. This is compatible with Deposits and Implications for Exploration. Edited by B. a preliminary 411 Ma age of hydrothermal rutile from a Dubé and P. Mercier-Langevin. Geological Survey of gold-bearing extensional quartz vein at Valentine Lake Canada, Open File 7852, pages 25-47. (Dunsworth and Walford, 2018). Colman-Sadd, S., Hayes, J. and Knight, I. 1990: The geology of the Island of Newfoundland. Map CONCLUSIONS 90-01, Scale: 1:1 000 000. Government of Newfound- land and Labrador, Department of Mines and Energy, The field data documented herein confirm that Antler Geological Survey Branch, GS# NFLD/2192. Gold Inc.’s Elm Zone mineralization and related veins rep- resents a structurally controlled gold-bearing quartz vein Currie, K.L. and Piasecki, M.A.J. system that is likely an extension of the well-endowed 1989: Kinematic model for southwestern Newfound- Valentine Lake structure to the southwest. However, where- land based upon Silurian sinistral shearing. Geology, as mineralization at Valentine Lake occurs in the structural Volume 17, pages 938-941. hanging wall of the Valentine Lake thrust zone, mineraliza- tion at Wilding Lake occurs in the structural footwall of the Dalton, B. and Scott, W.J. thrust zone. Footwall gold mineralization in association with 1995: First year assessment report on prospecting, geo- syn-orogenic clastic sedimentary rocks bears close resem- chemical exploration and geophysical interpretations blance to the major gold-bearing structures of the Abitibi for licence 4525 on claim block 8377 near the junction greenstone belt (see Bleeker, 2015). Deeper drillholes into of the Baie Despoir Highway and the Trans-Canada Rogerson Lake Conglomerate on the Antler property will be Highway, central Newfoundland, 2 reports. Newfound- important for determining its full economic potential, as land and Labrador Geological Survey, Assessment File rigid plutonic rocks, which are rheologically favourable for NFLD/2597, 1995, 26 pages.
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