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Macmillan Pass, Macpass Project - Tom, Jason, Boundary, End Zone |
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Yukon Territory, Canada |
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Zn Pb Ag
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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 Tom, Jason, End and Boundary Zone deposits of the Macpass Project are located in the Macmillan Pass district of the eastern Yukon Territory, close to the border with the Northwest Territories. Tom is approximately 6 km to the ENE of Jason. The Macmillan Pass district is around 100 km north-west of the Howards Pass deposits and 200 km east of the Anvil District (#Location: 63° 9' 16"N, 130° 15' 38"W).
Click here for a regional setting image. For detail of the geological setting of the Selwyn Basin and adjacent Mackenzie Platform see the Redstone Copper Belt record, in particular the Geological map of the Mackenzie Mountains, and the host sequence of the Howards Pass Zn-Pb deposits.
The mineralisation of the Macmillan Pass district is located on the eastern margin of the Selwyn Basin, near the transition from the flat lying carbonate dominated sequences of the Mackenzie/Interior Platform, to the folded, mainly clastic sediments of the Selwyn Basin. The Tom and Jason deposits are associated with several bedded, barite occurrences which are developed within the middle to upper Devonian "Black Clastic" or Earn Group. Barite occurrences are more extensively developed than the base metal deposits, but are generally barren to only weakly mineralised. All mineralisation is restricted to the transition between the lower assemblage of coarse clastics, mainly chert-pebble conglomerate and sand-banded argillites, to the overlying black carbonaceous argillite and siliceous shale. The deposits of the Macmillan Pass area are smaller, although of higher grade than those of the Anvil and Howards Pass districts (McClay, 1983; Carne and Cathro, 1981).
The stratigraphy of the Macmillan Pass district may be summarised as follows, from the base (after Grema et al., 2024):
• Road River Group, which overlies deep-water carbonates and shales of the Early to Late Cambrian Gull Lake Formation, and is composed of Early Ordovician to Late Silurian mudstone, chert and limestone units (Abbott and Turner, 1991; Abbott, 2013). It is divided into the Duo Lake, Steel and Sapper Formations. The Duo Lake Formation contains a graptolite biostratigraphy limiting it to ~479 Ma in the Late Tremadocian of the Lower Ordovician to ~423 Ma in the Early Wenlockian of the Silurian (Cecile, 1982). It comprises bedded siliceous mudstones and cherts that are overlain by a package of black siliceous mudstones and cherts (Abbott, 2013). The conformably overlying Steel Formation, comprises dark grey, wispy laminated and bioturbated mudstone (Gordey and Anderson, 1993). The youngest member of the group, the Sapper Formation, is composed of Late Eifelian, ~390 Ma (Fraser et al., 2021), recessive silty limestone and calcareous black mudstone (Abbott, 2013).
• Earn Group, which overlies the Road River Group, is divided into the Portrait Lake and overlying Itsi Formations (Abbott et al., 1986; Abbott, 2013). The Portrait Lake Formation, which ranges from Givetian to Famennian (387 to 358 Ma) in age, is constrained by conodont biostratigraphy (Abbott, 2013), and is host to the Tom and Jason deposits at Macmillan Pass. In the Macmillan Pass area, the Portrait Lake Formation (Cecile, 2000; Martel et al., 2011) is thought to be broadly a time equivalent to the Canol Formation in the Mackenzie Mountains to the east (Blusson, 1978; Carne, 1979; Abbott and Turner, 1991). It has been subdivided into the informal Niddery Lake, Macmillan Pass and Fuller Lake members, which are both underlain by, and interbedded with, the Macmillan Pass Volcaniclastics. The latter is an informal term describing carbonate-altered lapilli tuffs, tuffs, mafic flows, volcaniclastic breccias, sills and dykes that are variously interbedded with the clastic rocks of the Earn Group (Turner and Rhodes, 1990; Ootes et al., 2013; Fraser et al., 2021). These volcanic rocks are of Middle Devonian age (Turner and Rhodes,1990), although interbedded volcanic layers are also observed in the mudstones of the underlying Duo Lake Formation.
The Niddery Lake Member comprises cherty and black siliceous radiolarian mudstones that occur with barite and limestone lenses that may be up to 30 m thick (Abbott, 2013). The overlying Macmillan Pass Member is characterised by variable lithofacies distribution and thickness. It is broadly composed of grey to black, thinly laminated silty mudstone that is finely interbedded with sandstones. A thick chert pebble conglomerate within the unit forms a continuous sub-sequence with minor sandstone (Abbott, 2013). The overlying Fuller Lake Member, previously known as the Tom sequence (Abbott and Turner, 1991), is sandwiched between the overlying Itsi Formation and the Macmillan Pass Member. This Member comprises a 200- to 1500 m thick succession of carbonaceous mudstones that are commonly pyritic (Goodfellow et al., 1990). Pyritised radiolarian skeletons have been identified in the Portrait Lake Formation mudstones, and the abundance of cryptocrystalline quartz has been linked with biogenic silica sourced from high levels of primary productivity in the basin (Magnall et al., 2015).
Tom
The Tom deposit consists of two tabular bodies, Tom West and Tom East, that are 3 to 60 m thick, and are composed of finely inter-laminated chert, pyrite, sphalerite, galena, barite and black shale. Tom West ranges from 3 to 50 m in thickness and is laterally continuous over a strike length of 1100 m. The two tabular bodies are well zoned, both vertically and laterally. The basal sections tend to carry the highest Pb and Ag values, while the upper and marginal parts are relatively enriched in Zn and Ba. Cu, Pb and Ag rich stringer and alteration zones occur beneath the highest grade portions of the mineralised bodies (Carne and Cathro, 1981).
At the southern end of the Tom West body the mineralisation is high grade and composed of massive to poorly laminated barite-sphalerite-galena and pyrite, underlain by an interpreted cupriferous, silicified zone with pervasive pyrite and siderite veining. The massive ore is overlain by fine grained, finely inter-banded barite-sphalerite and galena with intercalated chert and minor carbonates. This banded mineralisation extends northwards from the underlying massive sulphides. The Tom East body is composed of discontinuous, high grade lenses of strongly deformed barite-galena and sphalerite (McClay, 1983).
Tom West lies on the western limb of a tight, north-south trending antiform, whereas Tom East occurs in a complex deformed and fault segmented limb of the same structure. The metamorphic grade is lower greenschist. Tom West dips steeply westwards and is locally tightly folded, with the banded sulphides folded in a similar fashion to the laminated wall rocks. There is a well developed axial plane cleavage, commonly paralleling bedding. In places the footwall and hangingwall of the mineralised layer are strongly sheared and bedding plane faults are mapped. At Tom East the deformation is more pronounced, and the banded sulphides are higher grade and more complexly folded (McClay, 1983).
Two phases of folding are recognised, an early isoclinal event which is particularly evident at the northern end of the Tom West deposit, while elsewhere, extension veins are abundant, particularly in the intercalated massive chert bands. The second stage of deformation produced open folds with local pressure solution crenulation cleavage within the folded barite-galena-sphalerite ore of the Tom West body. Barite is commonly recrystallised in these zones of deformation, with slightly elongate grains and a preferred orientation, forming a strong axial plane fabric to the first phase folding. During the phase 2 folding, the sphalerite remained fine grained and was little influenced, whereas the galena has been largely recrystallised, appearing to be interstitial between pyrite, sphalerite and barite. Framboidal pyrite with euhedral overgrowths is common in the black argillites near the deposit (McClay, 1983).
Within the massive sulphides of the southern end of the Tom West deposit, the dominant textures are massive colloform aggregates of pyrite with interstitial galena, sphalerite and minor pyrrhotite. The colloform pyrite has been overgrown, and in part replaced by large euhedral pyrite porphyroblasts. The pyrite has been micro-fractured and galena and carbonate deposited in the fractures (McClay, 1983).
Jason
Two mineralised lenses are also known at Jason, apparently at the same stratigraphic positions as those at Tom. The tenor, style and extent is also similar (Carne and Cathro, 1981). Makarenko et al., 2018 summarised the local geology at Jason, as follows. The deposit is hosted by a Devonian sequence that has been disrupted by faulting and folded into a series of upright tight west-trending, shallowly east-plunging folds (Turner, 1991). The position of the deposit is controlled by the location of the Jason Fault, a syn-sedimentary growth fault that brings older rocks of the Road River Group and lower Portrait Lake Formation of the Earn Group into contact with the Macmillan Pass Member and a stratigraphic package considered to be the lateral equivalent of the Tom Sequence (Goodfellow, 1991). The latter contains well developed sedimentary breccias, conglomerates and mass flow deposits (diamictites) that thicken towards the the Jason Fault, consistent with syn-sedimentary fault movement.
The Jason Main Zone is located on the northern limb of the east-plunging Jason syncline, while the Jason South Zone occurs on the southern limb. The latter zone comprises two separate horizons, whereas the Main zone is defined by a single lens. These two separate zones are considered to possibly be connected through the hinge of a syncline. These mineralised lenses can be divided into several distinct mineralisation facies, (after Turner, 1991):
• Pb-Zn-Fe sulphide facies - composed of massive, banded sphalerite-galena and galena-pyrite overlain by debris flow deposits containing clasts of earlier deposited massive sulphides;
• Barite-sulphide facies - interbedded fine-grained sphalerite, galena, barite, chert and ferroan carbonate forming the bulk of the mineralisation at Jason;
• Quartz-sulphide facies - interbedded sphalerite, pyrite, quartz and carbonaceous chert with quartz-celsian (barium feldspar) bands in the lower lens;
• Massive pyrite facies - massive pyrite beds interbedded with sphalerite, galena, chalcopyrite, pyrrhotite and quartz located near the Jason Fault; and
• Ferroan carbonate facies - massive beds of siderite and ankerite up to several metres across with irregularly distributed galena, sphalerite, pyrrhotite, pyrite, quartz, muscovite and pyrobitumen; spatially associated with a breccia pipe.
End Zone
The End Zone is 3.5 km northwest of Jason and hosts similar high-grade zinc-lead-silver mineralisation.
Boundary Zone
The significant Boundary Zone is located ~20 km NW to WNW of Jason. Drilling programs have encountered extensive mineralisation in the Boundary Zone in two different stratigraphic units:
i). the Late Ordovician to Early Silurian Duo Lake Formation, part of the Road River Group, which hosts the Howards Pass district mineralisation. Samples of the formation show it to be composed of grey to dark grey, finely laminated mudstones, which are variably cherty. Quartz constitutes a major proportion of the mineralogy and occurs as four main types. These include mostly <1µm detrital quartz that is a relatively minor constituent, and is dispersed in the matrix. Cryptocrystalline authigenic, chalcedonic quartz and <20µm micro-quartz that are the dominant two phases. Mega-quartz that is >20 µm is mostly found in veins or as pressure shadows around earlier mineral phases. The mudstones contain radiolarian-rich beds, often separated by mm- to sub-mm thick layers of very fine grained, radiolarian-poor, clay-rich layers. The radiolaria tests (i.e., skeletons) are partially preserved as cryptocrystalline and micro-quartz set in a cryptocrystalline quartz matrix containing microporosity and pyrobitumen. Pyrite is finely disseminated in the mudstone matrix. Bedding-parallel and high-angle stylolites are evident within the mudstones, often occurring both parallel to mudstone laminae and at the interface between the matrix and the silicified radiolarian tests,
ii). the Middle to Late Devonian Portrait Lake Formation of the Earn Group, which also hosts the Tom and Jason deposits (Gardner and Hutcheon, 1985; Bailes et al., 1986). As detailed above, this formation is subdivided into a number of units, the first of which is the Niddery Lake Member. In the Boundary Zone, this member comprises rhythmically intercalated, cm-scale, grey chert, pyrite and dark grey to black, sometimes silty, mudstone layers. The mudstone layers vary from fine <10 laminae/beds, up to 5 cm thick beds, giving the rock a banded appearance. The cherty layers comprise cryptocrystalline to micro-quartz, interbedded with layers that have radiolarian tests preserved as cryptocrystalline quartz, similar to the Duo Lake Formation. Over certain stratigraphic intervals, the Niddery Lake Member mudstones comprise interbedded, carbonaceous, radiolarian-rich layers, bedded micro-quartz, and nodular barite crystals. Barite is finely disseminated in the matrix, with phyllosilicate minerals, primarily illite, and is concentrated along laminae with differential compaction around the fluorapatite, barite and pyrite mineral crystals.
The succeeding Macmillan Pass Member comprises intercalated mudstone, conglomerate, volcaniclastics, and diamictite. The mudstones have interbedded silty and black carbonaceous layers with fine-grained stratabound pyrite. The pyrite is occasionally found as nodules and mm-sized grain aggregates. Subhedral to euhedral siderite crystals and minor dolomite are also disseminated in the mudstone matrix. The Macmillan Pass Member interbedded conglomerates contain well-rounded to subangular, pebble-sized clasts of quartz, chert and polylithic components. They can be clast- or matrix-supported, with quartz, siderite and sulphide minerals in the cement. Volcaniclastic beds are variably interbedded with the Macmillan Pass Member, dominated by lapilli tuffs. The clasts within the tuff are subrounded to angular, and vary from mm to a few cm in size, with hyaloclastic textures. Individual clasts and framework mineral grains in the lapilli tuffs are extensively altered and cemented by Fe carbonates and phyllosilicates. The diamictites found within the Macmillan Pass Member are composed of a diverse mixture of unsorted mudstone, conglomerate and volcanic clasts, within a sand- to clast-supported matrix. Barite, fluorapatite, siderite, pyrite, celsian and phyllosilicate minerals are common. Deformation features such as fractures, quartz veins, and dissolution seams (stylolites) are common in the diamictites.
The presence of multiple mineralised zones in different stratigraphic intervals is apparently unique among sediment hosted deposits in the Selwyn basin (Grema et al., 2024). Known mineralisation is distributed over a 2 km strike length and widths of 200 to 800 m, with drilled mineralisation in a central area 300 m long and a true thickness of up to 285 metres of >2% Zinc. Drilled intersections include 100 m @ 8.73% Zn within a 230 m @ 4.51% Zn interval. Mineralisation consists of sphalerite-siderite-pyrite and minor galena in veins, stockworks, interstitial disseminations, and as replacement of matrix and clasts within diamictites and chert pebble conglomerates. The mineralised zone is located adjacent to a major syn-sedimentary structure and contains large volumes of boulder diamictites indicating that the area underwent active tectonic extension during the formation of the basin, a similar setting at Tom and Jason areas. It is interpreted to be part of a distinct sub-basin that contains significant volumes of strongly siderite altered basaltic pyroclastics and lava flows within the same Earn Group formation that hosts the Tom and Jason deposits (Fireweed Metals, website, viewed March, 2023).
Mineralisation was deposited in three distinct stages (after Grema et al., 2024):
The Pre-mineralisation stage at Boundary is dominated by early diagenetic assemblages, including quartz, barite, pyrite, fluorapatite and phyllosilicates. In both Duo Lake and Portrait Lake Formations, this stage is characterised by two pyrite generations, as well as quartz, barite and phyllosilicate minerals. Pre-mineralisation pyrite (Py-0) is composed of framboids (Py-0a) and anhedral to subhedral pyrite (Py-0b) that form in the interstitial pore spaces of the mudstones, concentrated as stratiform pyritic layers, or as disseminations in the matrices of mudstones, conglomerates, volcaniclastics and diamictites. The Py-0a crystals are mostly <10 µm in diameter and can form aggregates that are up to 150 µm in diameter; whereas Py-0b crystals are relatively coarser grained, up to 120 µm) and often form an overgrowth on Py-0a (Grema et al., 2024).
The Mineralisation Stage I - which comprises stratabound fine-grained sphalerite, galena and pyrite with minor chalcopyrite, sulphosalts and barian mica. The sulphides of this stage were formed by barite replacement, nucleation on pre-mineralisation pyrite, and porosity exploitation during early biogenic silica transformation of opal-A to cryptocrystalline and micro-quartz in highly siliceous mudstones (which are up to 85 wt.% quartz). Dissolution-reprecipitation of quartz, and dissolution of barite, generated the permeability that was exploited. The sulphide minerals are hosted by the cherty and carbonaceous silty mudstones of the Duo Lake Formation and Niddery Lake Member of the Portrait Lake Formation. Sulphides of this stage are absent from the Macmillan Pass and Fuller Lake Members. In the Duo Lake Formation, stratabound steel-grey sphalerite (Sp-Is) is disseminated or occurs in bedding-parallel, radiolarian-rich layers ranging from <1 mm to 50 cm thick, often interbedded with barren, very fine grained mudstone. This Sp-Is broadly spherical and frequently occurs as pseudomorphic replacement of radiolarian tests, with grain sizes ranging from <10 µm to 1.5 mm, associated with micro-quartz and subhedral to euhedral crystals of pyrite (Py-I). In the Niddery Lake Member, stratabound sulphides occur in siliceous mudstone beds as irregular layers of grey sphalerite (Sp-Is), galena (Gn-I) and pyrite (Py-I). Sp-Is selectively and variably replaces radiolaria, barite and the mudstone matrix as <5 to 300 µm crystals (Grema et al., 2024).
The Mineralisation Stage II, is high-grade, and is volumetrically the major phase, occurring as layers, veins and breccias, some of which crosscut the mineralisation stage I stratabound sulphides. It was formed following the hydrothermal fluid-induced brecciation and cross-cutting veining that is prominent in the host rocks of both the Duo Lake and Portrait Lake Formations, and is accompanied by silicification and siderite alteration. The breccias and veins are infilled, and the fragments are cemented by sulphide minerals, phyllosilicates, mega-quartz and siderite. Breccia fragment sizes are variable, and mainly angular, and have sharp contacts with sulphides. The presence of kaolinite, pyrophyllite, quartz and fluorapatite suggests that hydrothermal fluids were likely F rich formed at temperatures of up to 240°C. Mineralisation stage II is best developed in the Macmillan Pass Member mudstones, conglomerates, volcaniclastics and diamictites. Banded colloform sphalerite (Sp-IIac) mostly occurs in veins and breccias of the Macmillan Pass Member, with up to 2.6 cm thick bands of crystals formed at the margins with wall rocks. The Sp-IIac occurs as alternating bands of dark brown to opaque and light brown to pale yellow crystals. Chalcopyrite blebs and chalcopyrite disease occur within the Sp-IIac crystals, whilst galena (Gn-II), siderite and dolomite are found as fine grained disseminations within the same. Coarse-grained anhedral pyrite (Py-IIa) is sometimes intercalated with Sp-IIac, or forms anhedral to subhedral crystals in interstitial pore spaces of the Sp-IIac. Py-IIa also forms massive layers in brecciated mudstones that commonly underlie the stratabound mineralisation. Two generations of coarse-grained sphalerite occur as overgrowths on Sp-IIac. These are not limited to the veins and breccias of the Macmillan Pass Member alone, but are also common in the massive pyrite replacement layers that underlie the stratabound mineralisation. The first of these is coarse-grained, porous, black to metallic brown sphalerite (Sp-IIb-mb), which overgrows Py-IIa and, rarely, the Sp-IIac in the veins, but is only a minor part of the mineralisation stage II sulphide assemblage. It is also intergrown with <25 µm fine-grained euhedral pyrite crystals. The second, and dominant of this coarse sphalerite pair, is a very coarse grained, up to 3 mm, red-brown sector-zoned sphalerite (Sp-IIc-sz) that was formed in veins crosscutting the Sp-Is stratabound layers. In veins, Sp-IIac sphalerite is almost always overgrown by Sp-IIc-sz. In contrast, in the breccia, Sp-IIc-sz is abundant and sometimes the only sphalerite present. It is occasionally rhythmically banded with red to colourless crystals. A coarse-grained, up to 1 cm galena (Gn-II), is commonly intergrown with Sp-IIc-sz in both veins and breccias. Other coeval mineral phases include fluorapatite, pyrobitumen and minor subhedral to euhedral mega-quartz (Grema et al., 2024). A third variety, a coarse-grained, pale-yellow to transparent sphalerite (Sp-IId-py) is found in both the Duo Lake and Portrait Lake Formations, postdating the earlier sphalerite and pyrite generations, and infilling cavities within the rocks. The individual crystals of Sp-IId-py range in size from 60 µm to mm-scale and are often associated with coarse, cm-scale mega-quartz and siderite crystals in veins and breccias.
Based on various relationships, Grema et al. (2024) have concluded that the multiple mineralising events of the Boundary Zone formed during a prolonged and intermittent period of fluid flow, spanning from diagenetic stages in the Lower to Middle Palaeozoic in the basin, possibly persisting to periods of Mesozoic Cordilleran-related deformation in the Selwyn basin.
Published resource/reserve figures for the Macpass Projects deposits include:
16 Mt @ 6% Zn, 4% Pb, 40 g/t Ag (Reserves, Tom, 1983, Goodfellow, et al.,1993).
10.1 Mt @ 7.5% Zn, 6.5% Pb, 80 g/t Ag (Reserves, Jason, 1983, Goodfellow, et al.,1993).
CSA Global was commissioned to prepare an independent estimate of Mineral Resources for the project as of 31 December 2017, as follows for Tom and Jason combined:
Indicated Mineral Resource - 11.21 Mt @ 9.61% Zn Equiv., 6.59% Zn, 2.48% Pb, 21.33 g/t Ag;
Inferred Mineral Resource - 39.47 Mt @ 10.00% Zn Equiv., 5.84% Zn, 2.48% Pb, 38.15 g/t Ag.
Mineral Resources at the Tom, Jason, End Zone and Boundary Zone deposits as at 4 September 2024 (Fireweed Metals website, viewed December 2024), were:
Indicated Mineral Resource - 55.98 Mt @ 7.27% Zn Equiv., 5.50% Zn, 1.58% Pb, 24.2 g/t Ag;
Inferred Mineral Resource - 48.49 Mt @ 7.48% Zn Equiv., 5.15% Zn, 2.08% Pb, 24.3 g/t Ag.
Within this resource, individual deposits contain:
Tom
Indicated Mineral Resource - 17.52 Mt @ 9.90% Zn Equiv.
Inferred Mineral Resource - 18.94 Mt @ 9.10% Zn Equiv.
Jason
Indicated Mineral Resource - 3.80 Mt @ 9.09% Zn Equiv.
Inferred Mineral Resource - 11.65 Mt @ 10.40% Zn Equiv.
End Zone
Indicated Mineral Resource - 0.34 Mt @ 16.15% Zn Equiv.
Inferred Mineral Resource - 0.44 Mt @ 8.76% Zn Equiv.
Boundary
Indicated Mineral Resource - 34.34 Mt @ 5.63% Zn Equiv.
Inferred Mineral Resource - 17.46 Mt @ 3.75% Zn Equiv.
The most recent source geological information used to prepare this decription was dated: 2024.
Record last updated: 30/12/2024
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.
Jason
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Ansdell K M, Nesbitt B E, Longstaffe F J 1989 - A fluid inclusion and stable isotope study of the Tom Ba-Pb-Zn deposit, Yukon Territory, Canada: in Econ. Geol. v84 pp 841-856
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Carne R C, Cathro R J 1982 - Sedimentary exhalative (sedex) zinc-lead-silver deposits, northern Canadian Cordillera: in CIM Bull v75, no. 840 pp 99-113
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Gardner H D, Hutcheon I 1985 - Geochemistry, mineralogy, and geology of the Jason Pb-Zn deposits, Macmillan Pass, Yukon, Canada: in Econ. Geol. v80 pp 1257-1276
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Grema, H.M., Magnall, J.M., Gleeson, S.A., Milton, J.E., Wudarska, A., Schleicher, A.M. and Schulz, H.-M., 2024 - Mineralogy and Paragenesis of the Boundary Zone Zn-Pb ± Ag Deposit, Yukon, Canada: in Econ. Geol. v.119, pp. 1833-1859. doi: 10.5382/econgeo.5115.
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Huston, D.L., Champion, D.C., Czarnota, K., Duan, J., Hutchens, M., Paradis, S., Hoggard, M., Ware, B., Gibson, G.M. Doublier, M.P., Kelley, K., McCafferty, A., Hayward, N., Richards, F., Tessalina, S. and Carr, G., 2023 - Zinc on the edge - isotopic and geophysical evidence that cratonic edges control world-class shale-hosted zinc-lead deposits: in Mineralium Deposita v.58, pp. 707-729.
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Magnall, J.M., Gleeson, S.A. and Paradis, S., 2020 - A New Subseafloor Replacement Model for the Macmillan Pass Clastic-Dominant Zn-Pb ± Ba Deposits (Yukon, Canada): in Econ. Geol. v.115, pp. 953-959.
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Magnall, J.M., Gleeson, S.A., Creaser, R.A., Paradis, S., Glodny, J. and Kyle, J.R., 2020 - The Mineralogical Evolution of the Clastic Dominant-Type Zn-Pb ± Ba Deposits at Macmillan Pass (Yukon, Canada) - Tracing Subseafloor Barite Replacement in the Layered Mineralization: in Econ. Geol. v.115, pp. 961-979.
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McClay K R, 1991 - Deformation of stratiform Zn-Pb(-barite) deposits in the northern Canadian Cordillera : in Ore Geology Reviews v6 pp 435-462
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Ootes, L., Gleeson, S.A., Turner, E., Rasmussen, K., Gordey, S., Falck, H., Martel., E. and Pierce, K., 2013 - Metallogenic Evolution of the Mackenzie and Eastern Selwyn Mountains of Canadas Northern Cordillera, Northwest Territories: A Compilation and Review: in Geoscience Canada, v.40, pp. 40-69, http://dx.doi.org/10.12789/geocanj.2013.40.005.
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