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Hemlo - Williams, Golden Giant, David Bell |
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Ontario, Canada |
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Au
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Super Porphyry Cu and Au
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IOCG Deposits - 70 papers
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All papers now Open Access.
Available as Full Text for direct download or on request. |
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The Hemlo district includes three main mines, Williams, David Bell and Golden Giant together exploit the Hemlo orebody. The district is located ~30 km east of Marathon, 350 km east of Thunder Bay and 330 km west of Timmins in southern-central Ontario, Canada (#Location= 48° 41' 47"N, 85° 54' 14"W).
The Hemlo deposit was discovered in 1982 after a long history of exploration, and all three mines had commenced production by the end of 1985 (Muir et al., 1991).
The combined production of these mines in 2000 made Hemlo the largest gold producing deposit in Canada with an output of 28.65 t (0.921 Moz). Williams alone was the largest single gold mine in Canada yielding 12.9 t Au.
The Hemlo deposit occurs within a generally east-trending, mixed assemblage of Archaean metavolcanic and metasedimentary rocks sandwiched between the major Gowan Lake and Heron Bay granitoid plutons to the north and south respectively. These supracrustal rocks are part of the Schreiber-Hemlo greenstone belt of the Wawa Sub-province of the Superior Province. The Schreiber-Hemlo greenstone belt appears to comprise of a basal pre-2697 Ma suite of tholeiitic basalt with minor ultramafic to mafic intrusions and flows. This suite is overlain by 2695 to 2688 Ma, calc-alkaline flows and volcaniclastic material, locally intercalated with sedimentary rocks. Quartz porphyritic units were emplaced between 2698 and 2693 Ma and preceded deposition of the sedimentary rocks in that area. Wackes to the southeast are younger than 2693 Ma but older than 2688 Ma. These observations are consistent with a regional sedimentary dominated sequence overlying, and in part derived from, the volcanic units. The sedimentary dominated rocks are locally intercalated with intermediate to felsic calc-alkaline volcanic rocks (as at the Hemlo gold deposit) and some sedimentary rocks may be distal facies equivalents of more proximal fragmental volcanic units. There are not any sedimentary or volcanic rocks known to be coeval with the late stage 2675 Ma plutonic rocks that intrude the belt (after Jackson et al., 1998).
The rocks in the Hemlo district have been regionally metamorphosed to amphibolite grades. An early metamorphism (temperatures of 500 to 600°C and pressures of 5 to 6 kbars) was probably accompanied by the intrusion of the Cedar Lake pluton and produced a mineral assemblage containing hornblende, kyanite, staurolite, garnet and micas from metasedimentary protoliths. A second metamorphic event (temperatures of 300 to 400°C and pressures of 1 to 3 kbars) produced an assemblage of actinolite, fibrolite, andalusite, calcite, garnet, epidote, chlorite and muscovite (Kuhns et al. 1994).
The Hemlo deposit is localised within a domain of generally east-west striking (110 to 115°), tightly folded, generally north dipping (60 to 70°) clastic sedimentary rocks with an intercalated suite of intermediate to felsic volcanic rocks. It lies in the hanging-wall of the transition zone from dominantly volcanic rocks to the south to dominantly sedimentary rocks in the north. The deposit is also only a few hundred metres north of the regional Hemlo reverse shear zone that separates the sequence of volcanic and the sedimentary rocks to the north, from the southern domain of mafic volcanic and clastic sedimentary rocks (Jackson et al., 1998).
Within the mine area, the host sequence has been divided into 8 lithological (not necessarily stratigraphic) units that may be repeated within the sequence, but are generally from south (mining footwall) to north (mining hanging wall) after Kuhns et al. (1988; 1994):
• Unit 1, Lower hornblende-bearing schists and amphibolite, and amphibolite to plagioclase-quartz-biotite-tremolitic-hornblende schist, which occurs as bands of 0.1 to >3 m thick interbedded with biotite schists of the footwall sequence. It has no appreciable alteration or mineralisation, except for limited epidote and pyrite with late fractures and brittle faults.
• Unit 2, Lower (southern) metasedimentary schists and granofels - defining the mining footwall sedimentary rocks, and are very similar to the sequence described under unit 7 below.
• Unit 3, Quartz porphyroclast muscovite schists - which contains porphyroclasts of quartz and feldspar, which represent deformed relicts of pre-existing phenocrysts. It occurs as several sub-types which are found over 50 to 80 m of the section between the structural footwall and hanging-wall schists in direct spatial association with mineralised zones. It locally hosts mineralisation, contains tourmaline and frequently pyrite, and locally contains biotite, V-Ti muscovite, microcrystalline garnet, barite, anhydrite, fluorite and rare scapolite. Anomalous gold is characteristic of the unit, with local ore grades. This unit, which is well developed at Golden Giant, thins down-dip and to the east in the David Bell mine, and is present as multiple zones to the west in the Williams mine.
• Unit 4, Ore zone-related biotite-hornblende-bearing schists - a strongly foliated and compositionally banded schist, subdivided on the basis of the presence or absence of lenticular fragments.
Subunit 4a contains 1-15% lenticular fragments of feldspar porphyry, 0 to 20%, 0.5 to 8 cm diameter microcrystalline grey quartz granofels, and 1 to 2%, 0.5 to 5 cm biotite schist, supported in a quartz-mica-feldspar-hornblende schist matrix.
Subunit 4b is a non-fragment-bearing quartz-mica-feldspar-hornblende schist. Biotite is dominant over muscovite in both sub-units, while green V-Ti muscovite is locally abundant. Minor calcite and rutile, and traces of garnet, scapolite, barite, and andalusite. In the upper part of the Golden Giant mine, unit 4 hosts gold mineralisation of up to ~8 ppm Au, although large portions contain little or no gold. The distribution of the unit has an overall antipathetic relationship with the bulk of the gold mineralisation and p,inches out rapidly with depth and to the east and west of the Golden Giant mine. Generally unit 4 is found structurally above unit 3, although the two units are locally interbanded.
• Unit 5, Ore zone schists and granofels - which has been sub-divided into three sub-units, namely,
Subunit 5a, a microcline-rich - exhibiting extreme textural heterogeneity, typically with a bluish-grey colour due to molybdenite, and fine-grained (0.05 to 0.6 mm), and a granoblastic mosaic-textured microcline-quartz granofels. It is tectonically fragmented and boudinaged, with molybdenite and native gold-rich granofels fragments supported in an Au-Mo poor granoblastic matrix of barite and/or pyrite, or transposed with the other subunits. Gold is locally intergrown with microcline.
Subunit 5b, a muscovite-rich - a white to yellowish-grey, foliated, microcline-muscovite-quartz schist. Molybdenite and native gold are characteristically foliated and intergrown with muscovite and green mica. This sub-unit, typically has flaser fabric and compositional banding (0.5 to >30 cm) defined by alternations with sub-units 5a and 5b.
Subunit 5c, a biotite-rich mineralised rock - composed of biotite-microcline-quartz schist containing molybdenite and native gold, which is texturally similar to subunit 5b. Gold and molybdenum are intergrown with biotite and green mica, and occur in both the fragments and the matrix. It seems to grade laterally into subunits 4a and 4b and typically has abrupt contacts with the muscovite dominated rock types such as some of the subunits of unit 7.
All three sub-units characteristically exhibit thin (1 to 20 mm) banding, small-scale S and Z folds, and lenticular fragments (boudins) of grey to blue-grey microcline-quartz-molybdenite-gold-bearing rock in a fine to coarse grained (0.5-5 mm) granular barite-quartz or pyrite-quartz granofels or schist matrix. Each is further divided on the basis of i). pyrite-rich, ii). barite-rich, and iii). quartz pod and vein-rich varieties of ore. Contacts between the mineralised subunits and between the ore and country rock are frequently gradational over several metres but are locally abrupt in areas of intense shearing.
• Unit 6, Fragment bearing hornblende-biotite schists - occurs as two heterolithic schist and granofels bands within the unit 7 schists. These bands of unit 6 rocks are each 20 to 40 m thick, 70 to 100 m apart, and 180 to 200 m structurally above the Main ore zone in the Golden Giant mine. Within these bands there are six lithological subunits:
Subunit 6a is a foliated, banded to massive plagioclase-biotite-quartz-tremolitic-hornblende schist which contains biotite-rich lenticular fragments (5 to 35%, 0.1 to 5 cm).
Subunit 6b is a fine-grained quartz-biotite-plagioclase-hornblende schist, similar to 6a, but devoid of lenticular fragments. It contains minor calcite, pyrite, and in some places contains 0 to 0.5%, 1 to 3 mm feldspar or quartz porphyroclasts.
Subunit 6c has a matrix composition similar to that of the previous subunits, but contains lenticular fragments of feldspar but it contains 5 to 40%, 0.5 to >10 cm lenticular fragments of feldspar porphyry and microcrystalline grey quartz granofels. In places the grey granofels contain visible molybdenite and rare visible native gold, and is similar in part to subunit 4a.
Subunit 6d occurs as thin 0.1 to 2 m thick bands of foliated muscovite-feldspar-quartz schist containing 5 to 10%, 2 to 4 mm, quartz porphyroclasts. It is locally weakly calcareous and contains trace green mica.
Subunit 6e is a pyritic (1 to 10% pyrite) equivalent of subunit 6d and is similar to pyritic subunits interlayered with biotite schists unit 7e. It locally contains anomalous gold and molybdenum and green mica.
Subunit 6f a feldspar-biotite-quartz schist containing 5 to 10%, 1 to 3 mm, feldspar 'eyes' or porphyroclasts. It locally contains lenticular fragments of biotite-rich schist, feldspar porphyry and microcrystalline grey quartz granofels.
• Unit 7, Upper (northern) metasedimentary schists and granofels - includes the bulk of the lower (southern or mining footwall) and upper (north, or mining hanging wall) schist rocks and is at least several kilometres thick. It comprises a diverse group of foliated and compositionally banded, fine- to medium-grained metasedimentary rocks. The hanging wall and footwall rocks are similar, but with some differences. Unit 7 is divided into 14 subunits, as follows:
Subunit 7al, Garnet porphyroblastic feldspar-biotite-quartz schist;
Subunit 7a2, Strongly foliated, anthophyllite porphyroblastic microcline-biotite-quartz schist;
Subunit 7b1, Strongly foliated, staurolite (garnet) porphyroblastic plagioclase-mica-quartz schist;
Subunit 7b2, similar to 7b 1, but chloritoid-rich, occurring as a chloritoid porphyroblastic plagioclase-mica-quartz schist;
Subunit 7b3, Banded kyanite-fibrolite porphyroblastic feldspar-mica-quartz schist - kyanite and sillimanite zones are almost exclusively found in close proximity to mineralised rocks (either the main and lower ore zones or the barren pyrite zones) and occasionally may contain up to 20% pyrite and 1 g/t Au;
Subunit 7c1, Strongly foliated, feldspar-muscovite-quartz schist - occurring throughout the Hemlo section but is most common in association with the ore zones and the barren pyrite zones where it can contains up to 6 g/t Au in close proximity to unit 5 and up to 1 ppm Au in the barren pyrite zones;
Subunit 7c2, Weakly foliated, muscovite-plagioclase-microcline-quartz schist - occurring as thin (0.5 to 5 cm), sometimes weakly gold mineralised, layers adjacent to the barren pyritic zones of subunits 7cl and 7e;
Subunit 7d, Lenses or pods and 1 to 10 cm thick bands of massive to weakly foliated biotite-microcline-quartz-hornblende schist-granofels that occurs throughout the sequence at Hemlo;
Subunit 7e, Laminated, locally calcareous, pyritic feldspar-muscovite-quartz schist (barren pyritic zone rocks), and anomalous in gold (up to 1 g/t);
Subunit 7f, The most abundant rock type in the Hemlo section, typified by laminated (1 to 10 mmm) and banded (1 to 5 cm) feldspar-biotite-quartz schist;
Subunit 7g, Similar to 7d but occurs as coarse grained granoblastic-textured, massive thick-bedded (1 to 15 m) microcline-biotite-tremolitic-hornblende-quartz schist - locally pyritic and gold bearing;
Subunit 7h, Hornblende-biotite-feldspar-quartz schist - an uncommon rock-type, interbedded with 7f;
Subunit 7i, Rounded feldspar-bearing biotite-plagioclase-quartz schist;
Subunit 7j, Muscovite-feldspar-calcite-quartz schist-granofels.
• Unit 8, Hornblende-bearing schists - subdivided into
Subunit 8a, Plagioclase-quartz-biotite-tremolitic hornblende±magnetite schist, after basaltic protoliths - the most abundant of the two unit 8 subunits, occurring as two 1 to 5 m thick principal bands in the hanging-wall of 7f and as thin horizons throughout the Hemlo section;
Subunit 8b, Fragment-bearing plagioclase-quartz-biotite-hornblende schist, also after basaltic protoliths.
The protoliths of the immediate hosts to the ore are interpreted to comprise greywacke, mudstone and minor conglomerate and fragmentals, and a quartz-eye porphyry unit of uncertain intrusive but more likely extrusive origin, but with which the mineralisation has a close spatial association. Post ore dykes of 2680 to 2690 Ma cut the sequence. All of the rock units strike sub-parallel to a strong SSE trending and north dipping S2 penetrative foliation which increases in intensity towards the Hemlo Shear.
Lin (2001) defines four generations of structures G1 to G4, which includes both ductile and brittle deformation. 'G' is used rather than 'D', because the four structural generations do not necessarily correspond to four discrete episodes of deformation. In the vicinity of the Hemlo deposit, these generations of structures were the result of at least two deformation events and comprised:
i). G1 - an early phase of small-scale F1 folds and possible low-angle normal or thrust faults. These structures are in close spatial association with, and are very similar in style to G2 structures. No macroscopic G1 structures are recognised, and it is likely that both generations are related to a single progressive deformation event;
ii). G2 - a major, regional, second phase producing small to large-scale, tight to isoclinal, generally NW- to NNW plunging F2 folds, accompanied by a penetrative planar axial schistosity and differentiated layering (S2), possibly associated with sinistral shearing and mylonitisation. G2 structures are the dominant features at Hemlo, where four such folds are mapped, the Cedar Creek, Williams Property, the Teck-Corona property fold and the Moose Lake fold. The S2 foliation is defined by the preferred orientation of mafic minerals (biotite and hornblende), clasts in conglomerate and volcaniclastic rocks, and by compositional layering with layers rich in biotite and/or hornblende alternating with those rich in feldspar ±quartz. S2 foliation dips steeply, generally 60 75° north or NE;
iii). G3 - dextral shear which locally produced SC mylonitic rocks and small- to medium-scale, generally NE- to east-plunging, F3 folds with axial planar schistosity and crenulation cleavage (S3). They are divided into G3a and G3b which produce F3a and F3b folds that are very similar in style, with no overprinting relationship between the two, other than a difference in hinge orientations; and
iv). G4 - small scale F4 faults and kink bands. The kinks are observed to overprint S2 foliation, but no overprinting relationship has been observed
between G3 and G4 structures.
The main mineralising event at Hemlo, the Au-Mo-K event, resulted in the introduction of Au, S, Mo, Zn, As, Sb, Hg, Tl and W and the associated alteration elements K, Si, Fe and V. This is interpreted to have taken place during the early stages of the major regional G2 deformation event, but prior to peak metamorphism. Pervasive potassic dominated alteration produced in a core of feldspathic alteration, largely composed of microcline-quartz, coincident with development of the ore zone and an outer halo of muscovite-quartz alteration. Significant pyrite with biotite and silica are associated with this alteration. Subsequent remobilisation of Au-Sb-Si is interpreted to have produced quartz veins with gold and stibnite, whilst an Au-Ca event resulted in redistribution of gold with calc-silicate alteration assemblages, and an Au-As-Hg pulse precipitated low temperature sulphide minerals such as realgar, orpiment and cinnabar from retrograde fluids. Molybdenite and the green vanadiferous mica roscoelite are the best visual mineralogical indicators of gold grades in the Hemlo deposit.
Enrichment of Au, Mo, and lithophile elements are interpreted to suggest the involvement of magmatic fluid that were channelled along the feldspar quartz porphyry-metasediment interface and mafic fragmental in the restraining bend of a regional sinistral, ductile shear zone. The barite horizon contributed to competency contrast and may have triggered gold precipitation. K, Si, Fe and V enrichment and Ca, Mg and Na depletion produced distinct alteration haloes both across and along strike from the deposit. The K enrichment is reflected as a strong radiometric anomaly. Associated pyrite produce a subtle but distinct very low frequency electromagnetic (VLF-EM) and induced polarization (IP) anomalies detected in both airborne and ground surveys. As, Sb, and Hg haloes are locally present as a result of metal redistribution during late alteration events. High Hg content is a distinguishing feature of Hemlo native gold mineralisation. Microcline related to alteration and mineralisation has high Ba and muscovite has high Ba and V. Rutile in the mineralised zone is enriched in V, W, and Sb. This paragraph is drawn from Cox, Valliant and Altman (2017, who referred to Barber (2010) as the source.
The Main ore zone occurs within a muscovite schist unit which can be traced from the David Bell Mine in the eastern part of the Hemlo area, through the Golden Giant Mine, to the western rim of the Williams Pit. It forms a 2.9 km long tabular body, concentrated on the northern margin of the porphyry, hosted both by the sheared porphyry of Unit 4 and adjacent fragmentals, extending to a depth of at least 1.35 km and 2.5 km down plunge. The thickness ranges from 2 m in David Bell to 50 m in Williams, but averages ~20 m. A Lower ore zone is found over strike length of ~600 m at depth on the southern contact of the porphyry, ~100 m south of the Main Zone in the central section of the main mines area. This zone is now believed to be a folded repetition of the Main ore zone. Other lesser mineralised zones lie either totally within the porphyry or within adjacent sediments.
Mineralisation comprises both fracture controlled and disseminated pyrite and molybdenite, commonly with associated barite, roscoelite, tellurides and quartz-stibnite-cinnabar-realgar veinlets. It is associated with intense K-feldspar alteration, grading outwards into muscovite within the porphyry and to alumino-silicates in the sediments. Relationships suggest the ore pre-dates the penetrative S2 foliation and may have been emplaced early in the geological history of the district.
Both the main and lower Hemlo ore zones are composed of feldspathic ore, sericitic ore and several minor styles. All are variably enriched in Mo as molybdenite, Au as native gold, As as realgar, Hg a cinnabar, Sb as stibnite and native antimony, Ba as barite and barium-rich microcline, V in the green vanadium-rich mica roscoelite, Tl, Zn and W (Harris, 1989; Powell and Pattison, 1997; Williams-Jones et al., 1998). Gold is disseminated in the ore zone.
The feldspathic ore is a massive to banded to fragmental, containing 40 to 55, locally up to 90% microcline, 10 to 40% quartz, muscovite,roscoelite, and minor biotite (Kuhns, 1986). It normally contains 3 to 35% pyrite and molybdenite, with the latter giving the rock a bluish color, a good indicator of gold. The feldspathic ore is typically high grade.
The sericitic ore is strongly foliated and is composed of 40 to 60% quartz, 15 to 30, locally up to 60% muscovite, feldspar, biotite and roscoelite (Kuhns, 1986). It contains up to 15% pyrite and traces of molybdenite. Typically, the sericitic ore is not as high grade as the feldspathic ore, which it tends to envelope. Gold-bearing quartz veins at Hemlo formed during the Au-Sb-Si remobilisation event detailed above, and have a widespread distribution but are volumetrically minor. No carbonate veins have been recognised (Lin, 2001).
In 1997, David Bell and Williams were jointly owned by Barrick-Homestake and Teck Cominco and had respective reserves of:
David Bell: 3.66 Mt @ 10.35 g/t Au (+ resource of 3.75 Mt @ 11 g/t Au),
Williams: underground 17.35 Mt @ 5.7 g/t Au (+ resource of 20.21 Mt @ 6.24 g/t Au),
open-pit 5.40 Mt @ 2.12 g/t Au (+ resource of 4.70 Mt @ 2.37 g/t Au).
Golden Giant is owned by Newmont Canada and had reserves of 4.78 Mt @ 9 g/t Au.
In the longitudinal section above, the Teck Corona claim is worked by the David Bell mine, Hemlo Gold by Golden Giant and Williams by the mine of the same name. The Quarter Claim was shared.
These reserves and resources amounted to 370 t (11.9 Moz) Au (Muir et al., 1995). The estimated resource+production at the Hemlo mines in 1988 was 585 t (18.8 Moz) Au, although this figure had only grown to 597 t Au in 2000. The Golden Giant mine was acquired by Newmont in 2001, and was exhausted and closed in 2006, after which rehabilitation took place. During its life, Golden Giant produced over 185 t of gold. David Bell and Williams is wholly owned by Barrick Gold, following the purchase of Homestake in 2001 and purchase of Teck's share.
Published Ore Reserves and Mineral Resources at 31 December, 2013 were:
David Bell underground mine and Williams underground and open pit mine
proved+probable reserve - 12.80 Mt @ 2.47 g/t Au for 31.7 t Au (Barrick Gold 2014), included within
measured+indicated resource - 52.84 Mt @ 1.13 g/t Au for 59.2 t Au (Barrick Gold 2014),
inferred resource - 1.52 Mt @ 4.9 g/t Au for 7.45 t Au (Barrick Gold 2014).
Remaining published NI 43-101 compliant Ore Reserves and Mineral Resources at 31 December, 2020 were:
Williams underground and open pit mine
proved+probable reserve - 9.60 Mt @ 4.8 g/t Au for 46.3 t Au (Barrick Gold 2021), included within
measured+indicated resource - 42.7 Mt @ 2.41 g/t Au for 59.2 t Au (Barrick Gold 2021),
inferred resource - 9.4 Mt @ 3.0 g/t Au for 28 t Au (Barrick Gold 2021).
The most recent source geological information used to prepare this decription was dated: 1998.
Record last updated: 5/11/2014
This description is a summary from published sources, the chief of which are listed below.
© Copyright Porter GeoConsultancy Pty Ltd. Unauthorised copying, reproduction, storage or dissemination prohibited.
Williams Golden Giant David Bell
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Brown P, Chong A, Kusins R, McNena K 1990 - Geology of the Golden Giant Mine: in 8th IAGOD Symposium, Field Trip Guidebook, Mineral Deposits in the western Superior Province, Ontario, Field Trip 9 Geol Surv Canada Open File 2164 pp 39-50
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Davis D W, Lin S 2003 - Unraveling the geologic history of the Hemlo Archean Gold deposit, Superior Province, Canada: a U-Pb geochronological study: in Econ. Geol. v98 pp51-67
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Fleet M E, Seller M H 1997 - Rare earth elements, protoliths, and alteration at the Hemlo Gold deposit, Ontario, Canada, and comparison with argillic and sericitic alteration in the Highland Valley Porphyry district, British Columbia, Canada: in Econ. Geol. v92 pp 551-568
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Heiligmann M, Williams-Jones A E and Clark J R, 2008 - The Role of Sulfate-Sulfide-Oxide-Silicate Equilibria in the Metamorphism of Hydrothermal Alteration at the Hemlo Gold Deposit, Ontario: in Econ. Geol. v.103 pp. 335-351
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Kuhns R J, Sawkins F J, Ito E 1994 - Magmatism, metamorphism and deformation at Hemlo, Ontario and the timing of Au-Mo mineralization in the Golden Giant mine: in Econ. Geol. v 89 pp 720-756
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Lin, S., 2001 - Stratigraphic and structural setting of the Hemlo Gold deposit, Ontario, Canada: in Econ. Geol. v.96, pp. 477-507.
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Michibayash, K., 1996 - Two phase syntectonic gold mineralization and barite remobilization within the main ore body of the Golden Giant mine, Hemlo, Ontario, Canada: in Ore Geology Reviews v.10, pp. 31-50.
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Muir T L 2003 - Structural evolution of the Hemlo greenstone belt in the vicinity of the world-class Hemlo gold deposit: in Can. J. Earth Sci. v40 pp 395-430
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Muir T L 2002 - The Hemlo gold deposit, Ontario, Canada: principal deposit characteristics and constraints on mineralization: in Ore Geology Reviews v21 pp 1-66
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Pan Y, Fleet M E 1992 - Calc-silicate alteration in the Hemlo Gold deposit, Ontario: mineral assemblages, P-T-X constraints, and significance: in Econ. Geol. v87 pp 1104-1120
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Pan, Y. and Fleet, M.E., 1995 - The late Archean Hemlo gold deposit, Ontario, Canada: a review and synthesis: in Ore Geology Reviews v.9, pp. 455-488.
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Powell W G, Pattison D R M 1997 - An exsolution origin for low-temperature Sulfides at the Hemlo Gold deposit, Ontario, Canada: in Econ. Geol. v92 pp 569-577
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Smyk M C, Schnieders B R and Muir T L 1990 - Field guide to the Hemlo area: in 8th IAGOD Symposium, Field Trip Guidebook, Mineral Deposits in the western Superior Province, Ontario, Field Trip 9 Geol Surv Canada Open File 2164 pp 26-38
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Tomkins, A.G., Pattison, D.R.M. and Zaleski, E., 2004 - The Hemlo Gold Deposit, Ontario: An Example of Melting and Mobilization of a Precious Metal-Sulfosalt Assemblage during Amphibolite Facies Metamorphism and Deformation: in Econ. Geol. v.99, pp. 1063-1084.
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