The Geological Framework of the Yukon Territory

Highlights 

Selwyn Basin Metallogeny 

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GEOLOGICAL SURVEY 

Cambrian to Devonian rocks of the Selwyn Basin and of the Earn Group host 

the world-renowned sedimentary-exhalative (SEDEX) deposits of zinc, lead, 

silver +/- barite of the Anvil district (Faro), Howards Pass and the Tom and 

Jason deposits of Macmillan Pass. Significant reserves remain and vast tracts of 

prospective stratigraphy remain under-explored and untested. 

Mineral Potential 

Over 800 known mineral occurrences are known to occur within the outline of 

Selwyn Basin, 19 of which are SEDEX deposits. An additional 89 occurrences 

have been described as SEDEX-type mineralization. Of the three main SEDEX 

districts listed above, only those of the Anvil district have been mined and all 

three still have potential for significant new discoveries. 

Exploration history and reserves 

The Anvil district was discovered in 1953. Mining occurred from 1969 to 1982, 

from 1986 to 1992, and from 1995 to 1998. In 1989, the Faro deposit was 

making Curragh Inc. the sixth largest zinc producer in the world. The combined 

pre-mining mineral resource was 120 Mt grading 5.6% Zn, 3.7% Pb, and 45-50 

g/t Ag. The Grum, Grizzly and Swim deposits still contain a geological resource 

of 67 million tonnes (this includes some mineable reserve and drill-indicated 

resource). The prospective contact remains locally untested, even close to 

known deposits, opening up the potential for new discoveries. Deposits of the 

Anvil camp are road accessible and are served by the town of Faro. 

In the Macmillan Pass area, the Tom claims were staked in 1951. A feasibility 

study was performed in 1985. Published mineable reserves for the Tom East 

and West zones are 9 283 700 tonnes grading 69.4 g/t Ag, 7.5% Pb and 6.2% 

Zn using a 7% combined Zn + Pb cut-off grade. The Jason deposit was staked 

in 1974 and is located at the same stratigraphic level as the Tom deposit. It 

contains an indicated mineral resource of 14.1 million tonnes of 79.9 g/t Ag, 

7.09% Pb and 6.57% Zn, using a cut-off grade of 8% combined Pb-Zn. The 

Tom and Jason deposits are accessible from the North Canol Road and by an 

airstrip located between the two deposits. 

Active exploration for lead and zinc in the late 1960s and 1970s led to the 

staking of the Howards Pass district in 1972. Geological resource (drill 

indicated) for the XY and Anniv deposits totals 110.5 million tons of 5.4% Zn 

and 2.3%Pb based on a 4.5% combined Pb-Zn cut-off; inferred reserves are in 

excess of 363 million tonnes. 

Other SEDEX deposits include the Clear Lake, as well as the Racicot and Tea 

barite deposits. The Rein and Dromedary occurrences are amongst numerous 

SEDEX occurrences in Selwyn Basin. 

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Capsule Description of SEDEX deposits 

SEDEX deposits consist of stratiform, bedded to laminated sulphides and barite 

in euxinic clastic marine sediments. Stratiform deposits are tabular to lensoid 

and may be deformed by subsequent folding and/or faulting. Multiple horizons 

may occur within one deposit. They occur in continental margin basins, 

associated with the development of second or third order basins from 

tectonism, subsidence and faulting (BCGS mineral deposit profile). Median 

tonnage for SEDEX deposits worldwide is 15 million tonnes; median grades are 

Zn- 5.6%, Pb- 2.8% and Ag- 30g/t. 

Geological setting 

Selwyn Basin is a continental margin basin characterized by the deposition of 

thick sequences of black carbonaceous shales in euxinic conditions and by 

development of second order basins through periodic extensional tectonism, 

subsidence and faulting. Deposition of the Earn Group marks the subsidence of 

the entire miogeocline, local uplift and faulting that caused the formation of 

localized secondary basins. Sedex mineralization occurs in close association 

with extensional tectonism producing deposition of coarse clastic sediments, 

syndepositional faults and coincident volcanism. Some epigenetic 

mineralization also occurs in this environment. 

The relationship between mineralization and volcanism is sometimes unclear. 

Some deposits may be described as transitional between true SEDEX and VMS 

deposits, such as the Matt Berry deposit. 

Major metallogenic events in the Cordillera are Early Cambrian, Early Silurian 

and Middle Devonian to Mississippian. Middle Devonian to Mississippian events 

are recognized worldwide (e.g. Red Dog in Alaska). Rocks of Selwyn Basin and 

Earn Group span this prospective time interval and host deposits of these ages. 

The Anvil deposits are Cambrian, Howards Pass is Silurian and Macmillan Pass 

is Devono-Mississippian in age. 

Geochemistry 

Extensive regional geochemical coverage is available for Selwyn Basin. 

Statistical treatment of data for Selwyn Basin outlines anomalies with a strong 

lithological control. 

Other deposit types 

The Marg volcanogenic massive sulphide (VMS) deposit is hosted in Devonian 

rocks of Selwyn Basin and contains 5.52 million tons of 4.6% Zn and1.76% Cu. 

This deposit has excellent exploration potential, as its limits have not yet been 

defined. 

Rocks of Selwyn Basin host numerous occurrences related to the Tombstone 

Plutonic Belt. This includes skarn deposits such as the Mactung Tungsten skarn 

(the largest tungsten reserve in the western world) and the Marn and Horn 

copper-gold skarns; distal vein deposits (Keno Hill district), replacement 

deposits (Brewery Creek, Harlan claims) and intrusive- and hornfels-hosted 

gold deposits (Dublin Gulch, Scheelite Dome, Clear Creek). These will be the 

subject of later compilations. 

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Selwyn Basin Metallogeny 

Introduction 

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The Yukon is endowed with world-renowned sedimentary-exhalative (SEDEX) 

deposits of zinc, lead, silver (barite) such as Faro (Anvil district), Howards Pass 

and the Tom and Jason deposits of Macmillan Pass (clicking on these links will 

bring you to the geology map for those areas). These deposits are hosted in 

Cambrian to Devonian rocks of Selwyn Basin and Earn Group. This overview 

summarizes the current understanding of the geology and metallogeny of 

these rocks, and focuses on the features that are indicative of potential for 

SEDEX mineralization. 

This overview is summarized and borrowed from several references: Abbott 

(1986), DNAG (various, 1991), Gordey (1993) and Murphy (1997); information 

on mineral deposits was compiled mainly from GSC O.F. 2169 (Abbott and 

Turner, eds., 1992) and CIM special volume 37, (Morin ed., 1986). 

Links in this text will take the viewer to selected portions of the Selwyn Basin 

Map, to related documents and to other websites. 

Definition of Selwyn Basin 

Selwyn Basin is well known as a geological province 

that spans the Yukon (Fig. 1). A basin formed by 

passive margin sedimentation, it is characterized by 

thick accumulations of clastic sediments, with a 

significant component of deep water black shales and 

cherts. These basinal rocks interfinger with, and are 

bound by, shallower water platformal carbonates. 

Several definitions of Selwyn Basin have been used in 

the literature. The original definition included the 

deep-water sandstones and shales as well as the 

fringing shallow water carbonate rocks. Later usage 

only included rocks that were deposited in a basin 

with known restrictions on both sides of the basin, 

which then limited Selwyn Basin to the known age 

range of the Cassiar Platform (late Silurian to early 

Devonian). A common usage is to simply define 

Selwyn Basin as a shale basin. Another usage is to 

include all rocks occurring in the geographical extent of these deep water 

clastics, including younger rocks, even intrusive ones. For a detailed discussion 

of the evolution of the definition, please refer to Abbott, 1986, and Gordey and 

Anderson, 1993, and Morrow, 2001. 

"Selwyn Basin", as is used in this document, follows the definition given by 

Gordey, 1993: "It refers to a region of deep-water offshelf sedimentation that 

persisted from late Precambrian to Middle Devonian time. Its basal deposits 

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Figure 1. Terrane map, from 

Abbott.

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consist of late Precambrian rift (-) clastics; it is overlain by rift clastics of late 

Devonian age. On its northeastern side are time-equivalent shallow shelf strata 

of Mackenzie Platform. Along its southwestern margin there developed in the 

Siluro-Devonian a carbonate-clastic shelf, the Cassiar Platform… Its 

southwestern limit is essentially the limit of the miogeocline as presently 

preserved (.)" in the Yukon. This definition addresses the offshelf facies 

between late Precambrian and lower Devonian, including the offshelf facies 

that mark the irregular transition into the carbonate platform. 

Spatially, Selwyn Basin is bound to the north by the Dawson Fault; it grades 

into platformal facies to the east (Mackenzie Platform) and southwest (Cassiar 

Platform); may be bound by a Mesozoic thrust fault separating it from Yukon- 

Tanana Terrane in the Anvil district; and is offset to the southwest by the 

Tintina Fault. 

Regional setting - the Cordilleran Miogeocline 

Selwyn Basin and Earn Group are part of the Cordilleran miogeocline. The 

miogeocline is defined as a westward thickening, then tapering, sedimentary 

prism that accumulated on the westerly sloping Precambrian basement of 

Ancestral North America from late Proterozoic to mid-Jurassic time (Gabrielse, 

1991). 

Proterozoic sequences: basement to Selwyn Basin 

The basement to the miogeocline includes Proterozoic and older crystalline 

basement rocks overlain by three unconformity-bound early to mid-Proterozoic 

sequences of carbonate and siliciclastic rocks: the Wernecke Supergroup, 

Pinguicula Group and Hematite Creek Group. The Wernecke Supergroup 

records two periods of basin subsidence and basinal infilling prior to 1.725 Ga; 

the Pinguicula Group is interpreted to represent rift sedimentation associated 

with the emplacement of mafic sills and related crustal extension and is 

bracketed between 1.59-1.38 and 1.270 Ga; the Hematite Creek Group 

consists of shallow-water carbonate and clastic rocks and is younger than 1003 

Ma (Thorkelson, 2000). Periods of sedimentation were separated by periods of 

uplift and erosion, and in some cases by deformation, magmatism and 

mineralization. 

Late Proterozoic (0.8-0.6 Ga) siliciclastic rocks of the Windermere Supergroup 

are the oldest exposed rocks in the miogeocline; they are only exposed in the 

inner or easternmost portion. They represent the development of a continental 

margin and the onset of passive margin sedimentation. 

Passive margin - Selwyn Basin 

From latest Precambrian or early Cambrian to early Devonian, the miogeocline 

was characterized by the development of two contrasting sedimentary facies 

belts, parallel to the continental margin. To the northeast, the inner 

miogeocline developed as a variably subsiding, carbonate shelf termed 

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Mackenzie Platform. To the southwest, deeper-water facies were deposited 

offshelf, forming an outer miogeoclinal basin on the flank of the continental 

margin, termed Selwyn Basin. 

Characterized by the deposition of offshelf deep-water clastics (shale, chert 

and basinal limestone), Selwyn Basin is bound by the Mackenzie Platform to 

the northeast, and, at least from late Silurian to early Devonian, by the Cassiar 

Platform to the southwest. Facies changes between deep-water clastic rocks 

(shale basin) and shallow-water carbonate rocks (platform) are transitional. 

This ’shale-out‘ marks the shelf edge or hinge line. 

Passive margin sedimentation 

was punctuated by periods of 

extension and tectonic 

instability. This caused 

widespread lateral migration 

of the shelf edge, and resulted 

in inter-fingering of shelf and 

offshelf facies (transitional 

units) as well as internal 

unconformities and scattered 

volcanism (Fig. 2). Irregular 

changes in the position of the 

Figure 2. Paleozoic migration of 

carbonate shelf edge, from Gordey.. 

facies boundary and local and 

intermittent extension resulted 

in the development of 

secondary rift basins such as the Misty Creek Embayment, the Richardson and 

Blackstone Troughs, and the Meilleur River Embayment. 

Turbidite basin - Earn 

Group 

From mid-Devonian to 

Mississippian, passive margin 

sedimentation in the outer 

miogeocline and platformal 

carbonate deposition in the inner 

miogeocline were interrupted and 

replaced by regional uplift and 

erosion followed by subsidence of 

the continental margin. A sudden 

influx of marine, turbiditic, chertrich 

clastic rocks (Earn Group) 

spread to the south and east from 

an uplifted source in northern 

Yukon, and to the east from uplifted western portions of Selwyn Basin. These 

clastics rocks blanketed all previous facies, covering Selwyn Basin sediments 

and onlapping onto the western Mackenzie platform (Fig. 3). Selwyn Basin, as 

a distinct topographic entity, no longer existed. 

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Figure 3. Distribution of Devono- 

Mississippian clastic strata, from 

Gordey.

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Sedimentation was accompanied locally by block faulting and felsic and mafic 

volcanism, and by widespread Ba and Pb-Zn-Ag-Ba mineralization. 

This abrupt change in sedimentation pattern has been attributed to a number 

of factors, including rifting, large-scale strike-slip faulting and the response to 

the compressive regime and uplift in northern Yukon created by the 

Ellesmerian orogeny. 

Clastic shelf 

From Mississippian to Triassic, marine shelf sedimentation resumed across the 

miogeocline, and is characterized predominantly by clastic sediments, some 

carbonates and numerous unconformities. Late Middle Triassic mafic sills 

intruded shallow marine sediments in the northwestern part of the area. 

Preservation of rocks spanning this time interval is sporadic. 

Mesozoic orogenesis and magmatism 

In Jurassic and Early Cretaceous time, the miogeocline was deformed by 

northeast-directed compression caused by plate convergence and the accretion 

of pericratonic terranes onto North America. The rocks of Selwyn Basin are 

relatively incompetent when compared to the carbonate rocks of the platforms, 

and responded by thrust faulting and the development of open to tight similar 

folds. 

Widespread Early to mid-Cretaceous granitic magmatism intruded the 

deformed rocks of the miogeocline. Five main intrusive suites are recognized: 

the Anvil (112-110 Ma), Tay River (98-96 Ma), Tungsten (97-92 Ma), South 

Lansing (95-93 Ma) and the Tombstone Suite (94-90 Ma). The McQuesten 

Suite was later emplaced around 65 Ma (Mortensen, 2000). The Tintina Fault 

zone, a late Cretaceous to Tertiary dextral strike-slip fault system with an 

estimated displacement of at least 450 km, and possibly up to 650 km, 

displaced the western margin of Selwyn Basin into what is now Alaska. 

Stratigraphy 

This section describes rocks of the outer miogeocline and the transitional units 

into the Mackenzie Platform, focusing on Selwyn Basin and the Earn Group. 

Significant sediment-hosted stratabound base-metal (SEDEX) deposits are 

hosted in these rocks: deposits of the Anvil camp (Faro) are hosted in 

metamorphic rocks that have been correlated with the Gull Lake and 

Rabbitkettle Formations; those of the Howards Pass district are hosted by the 

Duo Lake Formation of the Road River Group; and the deposits of the 

Macmillan Pass area are hosted in the Earn Group. 

This section is summarized from the systematic stratigraphic description 

outlined in Gordey (1993) and Murphy (1997). Appendix 1 outlines the table of 

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Formations; Figure 4 outlines the 

generalized stratigraphic and structural 

cross-section for the western part of 

Selwyn Basin. 

Offshelf facies 

Precambrian to Lower Cambrian 

Hyland Group (PCH) 

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The Hyland Group is the oldest exposed 

unit of Selwyn Basin. Informally known as 

the (youngest) Grit Unit (another Grit unit 

is part of the Windermere sequence), its 

base is not exposed. It is divided into two 

formations: a lower coarse-grained quartzrich 

turbidite succession and interbedded shales of the Yusezyu Formation and 

the overlying maroon to dark grey and green shale and limestone of the 

Narchilla Formation. 

Yusezyu Formation (PCH1) 

The Yusezyu Formation consists of several-kilometre-thick thick succession of 

medium- to coarse-grained quartzose sandstone and grit to quartz-pebble 

conglomerate, with interbedded shale and siltstone. The coarse clastic rocks 

(sandstone, grit, pebble conglomerate) were deposited in submarine fans from 

sediment gravity flows or turbidites. The uppermost part of the formation is 

variably calcareous, with silica cement locally replaced by carbonate cement. 

Limestone is a minor constituent (P_CH2) and can occur throughout the 

formation, but forms a thin, discontinuous member at the top of the formation. 

The upper part of the Yusezyu Formation is latest Precambrian based on the 

presence of primitive trace fossils from beneath the upper limestone member. 

Narchilla Formation (PCH3) 

The Narchilla Formation consists of several hundred metres of recessive 

maroon to dark-blue, grey, brown, buff and green weathering shale and 

siltstone, interbedded with fine-grained quartzose sandstone. Centimetre-scale 

colour banding within the shale often forms a characteristic striped pattern. 

Limestone beds may be present. In northern Lansing map area, the top of the 

Narchilla Formation contains mafic flows. The age of the Narchilla formation is 

late Precambrian to Early Cambrian, based on the widespread presence of the 

Early Cambrian fossil Oldhamia Radiata in the upper part of the formation. The 

Narchilla Formation is interpreted to be deposited below wave base in relatively 

deep water. The basal contact with the underlying Yusezyu Formation is 

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Figure 4. Stratigraphic 

section of Selwyn Basin 

(from Murphy).

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considered conformable. The top of the formation is defined at the conformable 

(-) base of the limestone conglomerate, buff slate, or volcaniclastic rocks of the 

Gull Lake Formation. 

The Hyland Group consists of thick turbidite deposits. The Yusezyu Formation is 

probably reworked from a pre-existing sedimentary source, perhaps itself 

derived from a granitic and possibly high-grade metamorphic terrane. 

Sedimentary textures suggest rapid erosion and deposition as sediment gravity 

flows (turbidites), such as in submarine fans, in shallow to moderate water 

depth. Sedimentary structures in the Narchilla Formation are consistent with 

gravity flows (turbidites). Limited paleocurrent data suggest a west or 

southwest source for the Hyland Group. Cambrian mafic sills intrude the 

Hyland Group and may be feeders to overlying Cambro-Ordovician basalts. 

Limestone and calcareous clastic rocks of the Hyland Group host replacement, 

vein and skarn mineralization 

Lower to Middle Cambrian 

Gull Lake Formation (lCG) 

The Gull Lake Formation is subdivided into three members: 1) a thin, basal, 

discontinuous limestone conglomerate with local archeocyathid clasts; 2) a 

dominant middle member of orange- to rust-brown-weathering laminated slate 

and siltstone to very-fine grained sandstone; and 3) an upper member of 

resistant, grey-weathering, thick-bedded, wispy-laminated, bioturbated 

calcareous to non-calcareous and dolomitic siltstone and mudstone. It locally 

contains mafic sills, flows or volcaniclastic rocks. In northern Niddery map 

area, their volume is significant and they are separated as the Old Cabin 

Formation. 

The age of the Gull Lake Formation is as old as Early Cambrian, based on the 

archeocyathid-bearing basal conglomerate and the presence of Bonnia- 

Olenellus trilobites; it is no younger than Late Cambrian based on its position 

beneath the Rabbitkettle Formation. 

The lower contact is generally considered to be conformable on the Narchilla 

Formation, with the possibility of a subtle disconformity. Sediments were 

mostly deposited below wave base in an offshelf, quiet water setting. The 

limestone conglomerate may represent debris flow from the time-equivalent 

platformal Sekwi Formation. The upper contact is sharply overlain by whiteweathering 

limestone of the Rabbitkettle Formation. Local truncation of Gull 

Lake strata indicates gentle pre-Rabbitkettle folding and/or faulting and a sub- 

Rabbitkettle unconformity. 

The SEDEX deposits of the Anvil district (e.g. Faro and Vangorda deposits) 

occur in the transitional upper part of the Mt. Mye Formation, a metapelitic unit 

that has been correlated with the Gull Lake Formation. It consists of noncalcareous, 

locally carbonaceous phyllite, marble and calc-silicate rocks with 

minor psammite and metabasite. 

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Late Cambrian to Early to Middle Ordovician 

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Rabbitkettle Formation (COR) 

The white-weathering basinal silty limestone of the Rabbitkettle Formation is a 

significant marker across Selwyn Basin. It unconformably overlies locally gently 

warped or truncated beds of the Narchilla, Gull Lake and Vampire formations. 

This unconformity is documented throughout the basin and is referred to as the 

sub-Late Cambrian unconformity or sub-Rabbitkettle unconformity. The 

Rabbitkettle Formation also occurs on the Mackenzie Platform, where it 

conformably overlies the Rockslide Formation. It is conformably below the dark 

shales and cherts of the Duo Lake Formation. 

At its type locality, the Rabbitkettle Formation consists of recessive, platy to 

thin-bedded, light-grey- to tan-weathering, wavy-banded or nodular limestone, 

silty limestone and siltstone. Elsewhere, other facies include: grey-orangeweathering, 

grey, finely crystalline nodular limestone; thin-bedded, orangeweathering, 

dark, finely crystalline argillaceous limestone; brick-red 

weathering, sugary, sandy dolostone; quartz sandstone and intraformational 

conglomerate; green volcanic tuff; and grey-green-weathering, laminated grey 

tuffaceous shale and variably argillaceous limestone. 

The lack of traction features and the presence of sedimentary features such as 

fine laminations, as well as the stratigraphic position west of shallow water 

carbonates, all indicate an offshelf, quiet water, below wave base depositional 

setting. The sub-Rabbitkettle unconformity is thought to mark a significant 

rifting event. The basinal setting of the Rabbitkettle Formation is attributed to 

subsidence of a thinned crust, following weak thermal uplift and erosion caused 

by rifting. The Rabbitkettle grades southward and westward into the Kechika 

Group of northern B.C. 

The Vangorda formation of the Anvil district consists of calcareous phyllite, 

metabasite, carbonaceous phyllite, chloritic phyllite and minor marble. It is 

correlated with the Rabbitkettle Formation, even though it is more argillaceous 

than the type Rabbitkettle and that no unconformity is observed at its base. 

The ore deposits of the Anvil camp (Faro deposit) occur at the transition 

between the Mt. Mye and the Vangorda formations. 

Cambrian-Ordovician 

(dempster) volcanics (informal) (COv) 

In the Dawson and Hart River areas, Middle Cambrian to Ordovician alkaline 

mafic volcanic rocks and volcaniclastic rocks with minor rhyolites are thought 

to represent a widespread rift event. This discontinuous unit includes mafic 

alkaline volcanic flow breccia, hyaloclastite breccia, agglomerate, and massive 

or pillowed flows. Some flows are porphyritic and contain large augite 

phenocrysts. In the Dawson map area, the sequence includes felsic volcanic 

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rocks. Dating is poorly constrained and gives at least two ages, one of which 

indicates a Windermere age, suggesting that some unrecognized Windermereage 

sediments and volcanics may be infolded or faulted in the Paleozoic 

sequence. 

The volcanic sequence is mainly interstratified with sedimentary rocks of the 

Road River Group. Au, Ag, and Pb mineralization is found in vein/faults cutting 

the volcanic package. 

Ordovician to Silurian 

Road River Group (ODR) 

Jackson and Lenz (1962) first used the term "Road River" as a formation name 

in the Richardson Mountains. The Road River Formation (CDR) consists of 

basinal limestone, chert and calcareous shales deposited in the Richardson 

Trough. Gabrielse (1973) used the term "Road River" in Selwyn Basin to 

describe mid-Ordovician to early Devonian black shale, chert and limestone 

overlying the Rabbitkettle Formation. The general usage now follows Gordey 

(1993) where the Road River is elevated to Group status and is composed of 

two formations: the basal dark-weathering Duo Lake Formation and the 

overlying tan- to orange-weathering Steel Formation. Other authors may 

further subdivide the Road River Group. For a comprehensive review of the 

usage of the term "Road River", please refer to Morrow, 2001. 

Early Ordovician to Silurian 

Duo Lake Formation (ODR1) 

The Duo Lake Formation consists of recessive, mostly dark, tan- to black- to 

blue- to bluish-white-weathering, black graptolitic shale, laminated chert and 

minor limestone, with minor silty shale and black- or tan-weathering light-grey 

siltstone. Proportions of shale and chert vary. The contact with the underlying 

Rabbitkettle Formation is sharp and conformable, but diachronous; the contact 

with the overlying Steel Formation is conformable and gradational over two 

metres. 

The black shale and chert were deposited in a quiet, euxinic offshelf setting 

starved from clastic input, at a depth greater than wave base. Graptolites yield 

ages ranging between Early Ordovician to early Late Silurian. Although poorly 

preserved, the presence of radiolaria supports a biogenic origin for the Duo 

Lake chert. In the Misty Creek Embayment, thick accumulations of mafic 

volcanic and volcaniclastic rocks of the Middle Ordovician Marmot Formation 

are interstratified with the Duo Lake Formation. 

In east-central Selwyn Basin, the large Howards Pass zinc-lead deposit is 

hosted in the carbonaceous chert and calcareous mudstone of the Duo Lake 

Formation. 

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Upper Silurian 

Steel Formation (ODR2) 

The Steel Formation is a distinctive thin unit of orange-brown-weathering 

pyritic, locally wispy laminated, siliceous, locally dolomitic mudstone to 

siltstone that conformably overlies the Duo Lake Formation. This contact is 

gradational over two metres; the contact with the overlying Portrait Lake 

Formation also appears conformable. 

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The Steel Formation was deposited in quiet-water basinal setting, at a depth 

greater than wave base. The wispy laminations represent horizontal burrowing 

and imply that oxygenated bottom waters had replaced the reducing euxinic 

conditions present during the deposition of the Duo Lake Formation. Graptolites 

indicate a definite Late Silurian age, but may range between mid-Silurian and 

early Devonian. 

Transitional facies 

The following formations are located along the inner margin (east and 

northeast) of Selwyn Basin, at the transition between basin and platform. They 

represent deep-water facies that are interstratified with platformal carbonates, 

the result of the migrating carbonate shelf edge. Only the offshelf facies are 

described here. 

The Vampire Formation (uP_CV) consists of dark-brown-weathering, thin- to 

thick-bedded siltstone, and dark brownish-grey-weathering, fine-grained quartz 

sandstone. Trace fossils indicate Precambrian to earliest Early Cambrian age. 

Sedimentary structures include planar laminae, load casts, and ball and pillow 

structures. The base of the formation is defined by the top of the highest 

orange-weathering dolomitic sandstone bed in the underlying dolomitic 

Backbone Range Formation. The Vampire formation was deposited in an 

offshelf, possibly slope, environment. It is equivalent to the Narchilla 

Formation, and also correlates with the upper member of the Backbone Ranges 

Formation. 

The Cambrian Rockslide Formation (CR) consists of recessive, dark-weathering, 

planar-laminated limestone. Additional facies include: nodular siltstone, oolitic 

limestone, and silty limestone. Textures include syn-sedimentary breccias and 

folds. The lower contact with the underlying Sekwi Formation is sharp but 

conformable. It is the lateral equivalent of the Gull Lake and Avalanche 

formations and underlies the platformal Rabbitkettle Formation. 

The Sapper Formation (ODR3) comprises recessive, thin-bedded, dark-grey to 

tan-orange-weathering limestone and silty limestone. Deposition was in an 

offshelf, below wave base setting. Fossils are abundant, indicate an age range 

from Late Ordovician to Middle Devonian, and support the diachronous nature 

of this unit. In some areas, the Sapper Formation cannot be distinguished from 

the overlying Funeral formation. It corresponds laterally to the Road River 

Group. 

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Turbidite Basin 

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At some point in the Devonian, the character of the continental margin 

changed from relatively passive and quiescent, to one of tectonic activity. 

Strata were locally uplifted and eroded, contributing chert-rich detritus to 

secondary rift-basins that formed during subsequent regional subsidence and 

marine transgression. The Earn Group records these events. 

The following section describes the Earn Group as well as coeval rocks 

interstratified with platformal facies (transitional units). 

Lower Devonian to Mid Mississippian 

Earn Group (DmE) 

The Earn Group records a regional marine transgression event, which is 

represented by the deposition of a turbidite basin sequence and local repeated 

uplift and subsidence. Definition of the Earn Group varies across Selwyn Basin, 

but current use of the term follows Gordey (1993) where the Earn Group is 

divided into two mapable units separated by an unconformity: the Lower to 

Middle Devonian Portrait Lake chert and shale unit, and the overlying Upper 

Devonian to Mississippian coarse clastic Prevost formation. 

Portrait Lake Formation (DmE2) 

The Portrait Lake Formation consists of gun-blue-weathering siliceous shale 

and thin-bedded chert with local chert-quartz arenite and wacke, pebbly 

mudstone, and chert-pebble conglomerate. Limestone beds are locally present. 

The top of the Portrait Lake Formation hosts a regionally extensive bedded 

barite horizon, several metres above muddy, chert-quartz sandstone and 

conglomerate. At least two intervals of barite deposition are inferred based on 

conodont data. The older interval is late Middle Devonian (Givetian) and occurs 

near Macmillan Pass; the younger interval is an early Late Devonian (Frasnian) 

horizon that occurs regionally and probably corresponds to one of the 

stratiform Pb-Zn- Ba horizons at Macmillan Pass. 

Throughout Selwyn Basin, the Portrait Lake Formation overlies various older 

units in different places, implying a regional disconformity and a diachronous 

basal contact. It conformably overlies the Steel Formation; it also overlies 

different levels of the Road River Group, the Rabbitkettle Formation, as well as 

the light-coloured transitional and shelf carbonates of the Funeral, Sapper and 

Haywire formations. 

The Portrait Lake Formation was deposited in a quiet, sub-wave base setting, 

characterized by generally low clastic influx and deposition of siliceous shale 

and chert. Chert-pebble conglomerate and other coarse clastics were deposited 

by sediment gravity flows (turbidites). It includes Early to late Late Devonian 

fossils. 

12/55

Prevost Formation (DmE2) 

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The Prevost Formation, of latest Devonian to mid-Mississippian age, overlies 

sharply and unconformably the siliceous shales and chert of the Portrait Lake 

Formation. It is composed of brown-weathering shale and siltstone and thick 

members of sandstone and chert-pebble conglomerate. 

Graptolites and conodonts indicate Early to late Late Devonian age. 

Sedimentary features in coarse clastics include massive bedding, graded 

bedding, rare Bouma sequence features, large shale clasts, chaotic bedding, 

and large groove casts. Clasts are chert, siliceous shale, and sandstone, some 

with blue quartz grains. Clast composition and structure indicate that the 

coarse clastics were eroded from an uplifted sedimentary terrane composed of 

quartz sandstone, shale and chert, possibly rocks of the Hyland and Road River 

groups. 

The deposition of coarse-grained clastic sediments was accompanied by local 

mafic and minor felsic volcanism, and syn-sedimentary faulting and 

mineralization. These volcanic rocks host the Marg deposit. 

The depositional environment was characterized by submarine fans and 

sediment gravity flows. Thick beds of coarse clastics were deposited within 

submarine fan channels, and shale was deposited between the tongues of 

coarse clastics. Sedimentary features indicate east to southeast paleoflow. 

Sediments may have been transported for at least 200 km. 

Transitional units 

The Grizzly Bear Formation (DB) consists of resistant grey-weathering, 

bioclastic (two-holed crinoids, stromatoporoids and corals) limestone. The 

basal contact with the underlying Sapper Formation and the upper contact with 

the overlying Funeral Formation are abrupt and possibly unconformable. Its 

thickness varies greatly along strike. Locally, it is too thin to be mapped 

separately, or pinches out. Where the Grizzly Bear Formation is absent, the 

Sapper and Funeral formations cannot be distinguished. Abundant fossils as 

well as stratigraphic position suggest an open marine setting, perhaps along 

shoals developed in the offshelf areas. It ranges in age between late Early 

Devonian and mid-Eifelian (early Middle Devonian). It is equivalent to the Earn 

Group, and correlates on the platform to the upper part of the Sombre and 

Arnica formations, and most of the Natla Formation to the east. 

The Funeral Formation (DH4) is an orange-weathering succession of dark, 

thin-bedded limestone and silty to shaly limestone. The contact with the 

underlying Grizzly Bear Formation is defined by an abrupt colour change, and is 

thought to be unconformable. Where the Grizzly Bear Formation is absent, the 

Funeral Formation cannot be distinguished from the Sapper Formation. 

Deposition was in an open marine shelf setting. It correlates to part of the 

13/55

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Portrait Lake Formation; its relative platform equivalent is the Headless 

Formation. 

The Natla Formation (DN) consists of thin-bedded to laminated turbiditic 

shale and fine crystalline limestone and chert. Fossil debris is common. The 

fossiliferous nature indicates an open marine depositional setting, possibly in a 

slope environment. The Natla Formation sharply and conformably overlies the 

Sombre Formation. Devonian age is constrained by conodonts and ranges 

between late Emsian to early Eifelian. It represents the offshelf correlative of 

the platformal dolostone of the Arnica and Sombre formations. It also 

correlates in part with the Grizzly Bear and the Sapper formations. 

Clastic shelf 

Mid-Mississippian to Jurassic rocks represent a re-establishment of a clastic 

shelf environment following the tectonic activity recorded by the deposition of 

the Earn Group. These rocks do not host any known syn-sedimentary 

mineralization and are described briefly. 

The Tay formation (MT) consists of recessive, dark, calcareous siltstone and 

shale, interbedded with thick, to thin, crystalline, dark limestone, commonly 

bioclastic. 

The Keno Hill quartzite (MK) consists of resistant, grey, massive- to thickbedded, 

locally banded quartz arenite to orthoquartzite, interbedded with 

variable amounts of black shale or calcareous phyllite and sandy limestone. 

Conodonts from rare limestone units indicate a Mississippian (Visean to 

Namurian) age. Various sedimentary environments have been proposed, all of 

which imply a shallow marine setting. The Keno Hill quartzite hosts the silverlead 

veins of the Keno Hill deposits. 

The Tischu formation (CPT) (informal), in part equivalent to the Keno Hill 

quartzite, occurs in eastern Selwyn Basin and unconformably overlies the 

Devionian Prevost formation (Earn Group). It consists of siliceous calcarenite, 

dolomite and minor quartzite, bioclastic limestone, shale, minor chert and 

chert-pebble conglomerate. It unconformably overlies the Devonian Prevost 

Formation. Conodont fauna indicate a Mississippian (Tournaisian to early 

Pennsylvanian) age. Its quartzite member is equivalent to the Keno Hill 

quartzite. It is interpreted to represent sand bar deposition on a shallow 

marine shelf. 

The Mount Christie Formation (CPMC) unconformably overlies the Tischu 

formation, and consists of tan-, orange- or red- and green-weathering, locally 

burrowed shale, siliceous shale, chert and minor sandstone, limestone and 

dolostone. Poor fossil control indicates a late Mississippian to Permian age. It is 

interpreted to be deposited in a relatively quiet below wave-base, with 

occasional pulses of coarse clastics. 

The Takhandit Formation (PJC3) consists of partially silicified and 

dolomitized skeletal limestone interbedded with chert, sandstone, and chert- 

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pebble conglomerate. Conodonts indicate a Permian age. This unit hosts the 

Marn skarn deposit. 

The Jones Lake Formation (TJ) consists of brown- to buff-weathering, 

calcareous, thin-bedded, fine-grained sandstone, siltstone and grey-brown 

shale. It is characterized by ripple cross-lamination, calcareous cement, detrital 

mica and bioturbation. The Jones Lake Formation is above and in 

unconformable contact with Mount Christie Formation. Conodonts yield a 

Triassic age. 

Youngest in this sequence is a dark shale, known as the Lower Schist (JB1) 

unit; it can be found in the Dawson and Mayo areas. It consists of thin-bedded, 

dark-grey argillite, slate and phyllite that is commonly carbonaceous or 

graphitic, platy to phyllitic quartzite, and minor limy quartzite. Fossils yield a 

Jurassic (Oxfordian) age. 

Triassic mafic sills intrude the Mississippian Keno Hill Quartzite in the Dawson 

map area. Sills in the Nash Creek map area intrude the Earn Group and are 

interpreted to be the same age. They represent the youngest pre-accretionary 

magmatic event in the miogeocline. 

Tectonic evolution of Selwyn Basin 

Selwyn Basin was the locus of deep-water sedimentation that lay southwest of 

a major carbonate platform from Late Precambrian to Devonian time. The 

dominantly thin-bedded siliciclastic rocks grade to the northeast into thickbedded 

carbonate sedimentary rocks of the variably subsiding Mackenzie 

Platform. From at least late Silurian to early Devonian, shallow-water clastic, 

volcanic and carbonate rocks of Cassiar Platform marked the southwestern 

margin of the basin. 

Local episodes of igneous activity occurred throughout the deposition of the 

sedimentary sequence. The association of widespread local accumulations of 

alkaline mafic rocks with Cambrian to Devonian unconformities or 

disconformities, and the local presence of coarse clastics are interpreted to be 

the result of several short-lived pulses of rifting. Volcanism is interpreted to be 

the result of extension accompanying thermal subsidence, and contraction of 

the lower crust following thermal uplift due to rifting. 

From Cambrian to Silurian time, migration of the shelf edge caused 

interstratification of basinal and platformal facies, the progradation of basinal 

rocks into the platform and the formation of a series of satellite sub-basins that 

occur mostly on the Northwest Territories side of Selwyn Basin (Misty Creek, 

Meilleur River and Prairie Creek embayments). Deep-water troughs 

(Richardson and Blackstone troughs) were also formed and are found 

extending into, or enclosed within, the carbonate platform. Dominantly mafic 

and alkaline volcanic rocks are associated with the sub-Late Cambrian 

unconformity and also occur in Ordovician, Silurian and Devonian times. Rifting 

events are inferred in each case. Mid-Devonian rifting and/or wrench faulting 

resulted in a regional marine transgression that abruptly terminated the 

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Selwyn Basin phase of passive margin sedimentation. Coarse-grained clastic 

and siliceous sediments were deposited across the former shelf edge, locally 

accompanied by mafic and less abundant felsic volcanism. 

Selwyn Basin - passive margin phase 

The coarse clastic turbidites of the Upper Precambrian to Lower Cambrian 

Hyland Group are the oldest exposed rocks of Selwyn Basin. They represent 

thick accumulations of sediments in submarine fans that were fed from an 

unidentified, rapidly uplifted source area and deposited in a deepening basin. 

Marginal uplift and sedimentation are interpreted as manifestations of the 

onset of a major rifting event. The overlying Lower Cambrian Gull Lake 

Formation marks offshelf quiet water setting with some clastic input from the 

Mackenzie Platform. Local mafic volcanic rocks at the base of the Gull Lake 

Formation and the possibility of a disconformity at that stratigraphic level 

suggest a less pronounced rift event in late Early Cambrian time. 

The sub-Rabbitkettle or sub-Late Cambrian unconformity is a basin-wide 

feature thought to result from thermal uplift and erosion caused by a Middle to 

Late Cambrian rifting event. Subsequent widespread Cambrian mafic volcanism 

lasted into the Ordovician. 

The SEDEX deposits of the Anvil district occur during this time interval, at the 

transition between the Mt Mye and Vangorda formations, which have been 

respectively correlated to the Gull Lake and Rabbitkettle formations. 

From Late Cambrian-Ordovician to 

Silurian time, the Road River Group 

was deposited in euxinic deep water 

conditions. The Lower Ordovician to 

Silurian Duo Lake Formation hosts 

the large Howards Pass zinc-lead 

deposit in east-central Selwyn Basin. 

The Upper Silurian Steel Formation 

was deposited in a deep, but 

oxygenated environment. Some local 

tectonic instability is manifested by 

the sporadic eruption of Cambrian to 

Ordovician mafic alkaline volcanics 

and the migration of the shelf edge. 

The shelf edge was broken by a 

series of embayments, basins and 

troughs within which deeper-water 

facies extended from the main part of 

Selwyn Basin into the platform 

(Richardson and Blackstone troughs, 

Misty Creek and Meilleur River 

embayments (Fig. 5). Several arches 

(e.g. Mackenzie and Ogilvie arches) 

16/55 

Figure 5. Tectonic 

elements, from 

Abbott.

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exerted a degree of influence on the distribution of sedimentary facies. To the 

south, Selwyn Basin was connected to the Kechika Trough of the southern 

miogeocline, which is situated in northern British Columbia. 

The Misty Creek Embayment (Fig. 5) formed during Middle Cambrian and 

younger extension. The Hess River flysch sequence records uplift and erosion 

of the flanks of the embayment. Deposition of the Rabbitkettle Formation was 

followed by the eruption of the Middle Ordovician to Middle Devonian volcanics 

of the Marmot Formation that were deposited along the Duo Lake Formation 

(Road River Group). The Meilleur River Embayment was a large semi-circular 

embayment of Selwyn Basin that extended into the southern Mackenzie 

Platform from Ordovician to Silurian time. The Prairie Creek Embayment 

developed in Late Silurian as an eastern satellite depression in the Meilleur 

River Embayment and was the focus of carbonate sedimentation while 

deposition of Road River shale continued in the rest of the Meilleur River 

Embayment. Both the Meilleur River Embayment and the Prairie Creek 

Embayment were located in the central part of the Liard Depression, a longlived 

depocentre that developed in the Ordovician and continued into Devonian 

time. 

Earn Group- turbidite basin phase 

The final and most widespread rifting event in the miogeocline occurred in 

Devono-Mississippian time. Rifting or wrench faulting along the outer 

miogeocline caused a dramatic change in pattern of sedimentation. Tectonism 

may have been associated with a back-arc setting, inboard to a pericratonic 

Devono-Mississippian arc (Yukon-Tanana Terrane) that formed on the western 

margin of North America; the change in sedimentation is coincident with the 

age of magmatism on the arc. Widespread Middle to Late Devonian and early 

Mississippian transgression created a deep marine basin. Shale was deposited 

across the pre-existing platform-basin transition and well into the Mackenzie 

Platform to the east. At the same time, to the west, the basin was broken by 

rift zones that controlled deposition in submarine fan complexes of coarse 

clastics of the Earn Group. Exhalative barite and sulphides were deposited in 

this setting, forming significant SEDEX deposits in the Macmillan Pass area, at 

Clear Lake and in the Kechika Trough. 

The deposition of coarse-grained clastic sediments was locally interbedded with 

volcanic assemblages that include mafic and felsic flows and tuffs. Less 

abundant felsic volcanism occurred on Cassiar Platform and near the Marg VMS 

deposit. Shale-hosted nickel-sulphide mineralization was also deposited during 

this time interval, as seen at the Nick occurrence. 

17/55

Structure 

Murphy, 1997, outlines the generalized stratigraphic and structural crosssection 

for the western part of Selwyn Basin (see Figure 4). 

Y 


Deformation of Selwyn Basin rocks is dominated by Mesozoic structures. 

Although less obvious, pre-Mesozoic synsedimentary faults are significant as 

they control the development of secondary sedimentary basins and focus 

volcanism and SEDEX mineralization. Where preserved, these structures can be 

recognized from contact relationships. In other cases, these older structures 

may be cryptic, as they are often overprinted by younger structures. Other 

brittle structures, both pre- and post-Mesozoic, control the north-northeast to 

east-northeast steeply dipping veins and vein faults. 

Mesozoic deformation style is controlled by the incompetent nature of the 

dominant basinal shaly facies. The rocks deformed internally as a 

homogeneous mass forming the thrust and fold belt called the Selwyn Fold 

Belt. The Yukon portion of the Selwyn Fold Belt is bounded to the northeast by 

the carbonate platform edge and the coincident Mackenzie Fold Belt, and to the 

southwest by the leading edge of accreted terranes and by the dextral 

transcurrent Tintina fault. 

Mesozoic deformation reflects response to largely northeasterly directed 

compression. Timing of deformation is constrained: it is younger than the age 

of the youngest rocks cut by thrust faulting and folding (Jurassic) and is older 

than the age of non-foliated intrusions that cut the deformed strata as well as 

thrust faults (mid- and Late Cretaceous). Slight variations in these ages occur 

throughout the belt with variation in age of intrusive activity and age of 

deformed strata. 

The fold belt is characterized by large-scale thrust faulting, open to tight 

similar folds, imbricate fault zones, and the development of axial planar slaty 

cleavage. Competent cherts deformed as chevron folds or isoclinal folds, 

accommodating a significant amount of shortening, with detachment surfaces 

in less competent strata. In contrast, the thick sequence of competent 

carbonate rocks of the Mackenzie Platform buckled forming large concentric 

folds and thrust faults; these rocks also lack the slaty cleavage 

Structural trends parallel the arcuate Paleozoic shale-carbonate facies 

boundary. In some areas, complex internal crumpling and faulting may have 

doubled or tripled stratigraphic thickness without destroying gross stratigraphic 

integrity. 

Faults within Selwyn fold belt have two main orientations: 1) north- to 

northeast-trending faults, which are oblique to the fold trend (< 10 km strike 

length and

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In western and central Selwyn Fold Belt, strata are folded and imbricated by a 

series of moderately south-dipping, northerly-directed thrust faults (see Figure 

4). 

Three principal thrust faults are, from south to north and from oldest to 

youngest: the Robert Service Thrust, the Tombstone Thrust and the Dawson 

Thrust. These faults are more than 200 km long and are inferred to root in a 

single detachment in the Yusezyu Formation of the Hyland Group, with faults 

cutting progressively deeper in the section from north to south. The intensity of 

deformation, amount of shortening, and grade of metamorphism all increase 

from north to south. 

The Robert Service Thrust extends from the Dawson map sheet to the northern 

end of the Mayo map area. In Mayo map area, the Robert Service Thrust sheet 

is deformed within the Tombstone Strain Zone (Fig. 6). 

The Tombstone Thrust parallels the Robert Service Thrust and is characterized 

by the development of a thick, highly strained ductile shear zone in its hanging 

wall, called the Tombstone Strain Zone (TSZ) that gradually grades upward into 

non-strained rocks and juxtaposes progressively older rocks towards the east 

in both hanging and footwalls, with metamorphic grade increasing toward the 

east. The thrust probably links into west-northwest-striking dextral strike-slip 

faults of the Macmillan Pass area. 

The Tombstone Strain Zone is characterized by prominent foliations and 

lineations, lenticular compositional layering, shear bands, and folding, as well 

as having a higher metamorphic grade than rocks outside the zone. TSZ 

structures and fabrics deform earlier folds and structures resulting in the 

folding and imbrication of the earlier Robert Service Thrust. Many kinematic 

indicators suggest top-to-the-northwest displacement, supported by vergence 

of asymmetrical folds. The TSZ is itself folded by open regional-scale folds. 

The Dawson Thrust fault is a linear 

Mesozoic thrust more than 200 km 

long that sharply juxtaposes basinal 

rocks on its south side to a shallowwater 

platformal sequence on its 

north side (Figure 6). It forms the 

southern boundary of a Lower 

Paleozoic shelf-carbonate sequence 

and the northern boundary of 

Selwyn Basin. The Ancestral 

Dawson fault strongly influenced 

the emplacement of mafic volcanic 

and intrusive rocks through much of 

the Paleozoic, Late Proterozoic and 

possibly earlier. These rocks are in much greater abundance near the Dawson 

Thrust fault than in equivalent sequences elsewhere. Even though the Dawson 

thrust marks a significant and sharp boundary between contrasting 

sedimentary environments, it is interpreted to represent a moderate amount of 

shortening, with displacement being no greater than displacement on other 

thrust faults. Offset across the fault could be as little as two to four kilometres. 

19/55 

Figure 6. Cross section 

through Dawson Fault, from 

Abbott.

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The Dawson Thrust is interpreted to be an ancient underlying basement 

structure, which repeatedly influenced patterns of sedimentation, igneous 

activity and faulting, at least since later Proterozoic time. 

In the Anvil Range and to the northwest, structure is dominated by moderate 

southwest-dipping or flat-lying strata imbricated by several large northwesttrending, 

northeast-directed thrust faults. Detachment surfaces are at the base 

of Devono-Mississippian chert-pebble conglomerate, or at the base of thick 

Ordovician volcanics. 

In Eastern Selwyn Basin, strike-slip and normal faulting mark the contact with 

the underlying Proterozoic assemblages. In the Nahanni map area, Devono- 

Mississippian steeply dipping, normal or reverse, syn-depositional faults, 

exhalative barite, and Ag-Pb-Zn mineralization suggest an extensional or 

transtensional regime. Mesozoic deformation is pre Late-Cretaceous and post 

mid-Triassic. Further north, folding is Early Cretaceous. Some faults are 

truncated by mid-Cretaceous plutons; others postdate plutonism. 

In the Macmillan Pass area, the Macmillan fold belt has a westerly trend and is 

thought to reflect a deep-seated Devonian fault zone. Folding is tight and a 

narrow, imbricate fault zone of southerly directed, east-west-trending thrust 

faults repeats Lower Cambrian to Devonian stratigraphy. South of the imbricate 

belt, open to closed folds and steep faults are the dominant structures. Some 

of the steep faults may have been active in the Devonian, forming grabens, 

and later exerted control on development of the Mesozoic imbricate belt. 

Northeast from the imbricate belt, the structural trend bends from northerly to 

a northwest-southeast orientation. In southwest Macmillan Pass area, the 

structure is dominated by small- to intermediate-scale chevron folds in thinbedded 

chert of early Paleozoic age. The chert succession has been shortened 

and thickened, but not tilted or imbricated. Displacement was accommodated 

in the bounding incompetent shales. 

Several short-lived pulses of rifting are marked by Cambrian to Devonian 

unconformities and volcanism. Cretaceous brittle structures control the northnortheast 

to east-northeast, steeply dipping veins and vein faults such as those 

of the of the Elsa-Keno Hill silver-lead deposit. These post-date Tombstone 

Strain Zone fabrics as well as Cretaceous intrusions, but control the 

emplacement of late dykes. 

Metamorphism 

Regional metamorphism is lower greenschist facies. Slightly higher 

metamorphic grade is observed in rocks in the Tombstone Strain Zone where 

sedimentary and igneous rocks are metamorphosed to psammite, phyllite, 

slate, siliceous phyllite, chlorite-muscovite phyllite, metabasite, orthoquartzite 

and marble. Maximum depth of burial in the Nahanni map area is estimated at 

less than 5 km for the Steel Formation and less than 10 km for Hyland Group, 

giving a maximum pressure of 2.8 kb. 

Contact metamorphism is evident around Cretaceous plutons. Contact aureoles 

20/55

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are up to several kilometres in diameter, producing calc-silicate, pelitic and 

siliceous hornfels. Porphyroblasts include kyanite, andalusite, plagioclase, 

garnet, cordierite, sillimanite and chloritoid. Pelitic hornfels zones are often 

gossanous, as a result of the oxidation of the disseminated sulphides (mainly 

pyrrhotite) that is present in the hornfels. Pressure during pluton emplacement 

was no greater than 3.5 kb. 

Mineral Deposits 

Syngenetic deposits in rocks of Selwyn Basin and Earn Group span a range of 

ages, size and grade, mineralogy, tectonic environments and levels of 

deformation, alteration, metamorphism and preservation. The large, significant 

deposits are distributed on either side of Selwyn Basin. 

Some elements are common between these deposits. Mineralization occurs at 

or near the contact between two formations, marking a pause or transition in 

between depositional environments. Deposits are usually hosted in fine-grained 

clastics in linear second- or third-order sediment-starved anoxic basins. In all 

cases, mineralization is inferred to be related to a local rifting event, although 

only in Macmillan Pass is this well documented. Throughout the evolution of 

Selwyn Basin, several local and episodic extensional events are documented. 

In the best of cases, clear evidence of rifting is found to be coincident with 

extensional faulting, deposition of coarse clastics, volcanism and 

mineralization. SEDEX deposits occur as the exhalative fluids are channeled by 

syn-sedimentary faults and precipitate on the sea floor. 

Some mineralogical, chemical and textural zoning is usually present. Synsedimentary 

ores are laminated and interbedded with host rocks, and can be 

replaced and brecciated by later ore fluids. 

Igneous rocks can be important controls for some syngenetic deposits. 

Volcanism is quite often found to be coeval with mineralization such as in the 

Anvil and Macmillan Pass district. Volcanogenic mineralization is present at the 

Marg deposit; it is discussed below as it represents another end of the 

spectrum of exhalative activity. Some occurrences within Selwyn Basin have 

characteristics of both SEDEX and VMS deposits and would be classified as 

transitional between the two models. 

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The comparative table below highlights the similarities and contrasts between the 

four deposits highlighted in this document. 

Anvil district Howar 

ds 

Pass 

Age Cambrian Silurian 

(Llandover 

y) 

Host 

Formation 

Mt Mye/ 

Vangorda 

contact 

(correlated to 

Gull Lake/ 

Rabbitkettle) 

Main Minerals pyrite 

(sphalerite, 

galena, barite, 

minor 

pyrrhotite) 

Ore Zoning Anvil cycle 

siliceous at 

base, pyritic 

above, barite 

in core 

District 

Approximate 

Size 

Pre-mining: 

120 Mt 

5 deposits 

relatively high 

grade and 

large tonnage 

Macmillan 

Pass 

Marg 

Devonian Devono- 

Mississippia 

n 

Road River Earn Group Earn Group 

sphalerite, 

pyrite, and 

galena 

Active 

Member: 

zoned 

vertically 

and 

laterally; 

Zn/Pb+Zn 

increase 

from base 

to top and 

from 

centre to 

margin; 

Hg/Zn in 

sphalerite 

increases 

from 

centre to 

margin; 

high-grade 

core 

where 

thickest. 

Geological 

: 110 Mt 

inferred: 

360 Mt 

2 deposits 

22/55 

galena, 

sphalerite and 

barite 

Zoning of 

metal ratios: 

hydrothermal 

facies and 

sedimentary 

textures 

upward and 

away from 

vent and 

related synsedimentary 

fault. 

Geological: 17 

Mt 

calculated on 

2 deposits; 

high grade, 

small tonnage 

pyrite, sph, 

cp, galena, 

tetrahedrite 

and asp 

Vent: 

carbonate, 

massive 

pyrite with 

high Cu/Pb 

and Zn/Pb 

ratios; 

footwall: 

carbonateqtz-pysericite 

schist. 

Geological: 

5.5 Mt 

1 deposit

low grade, 

large 

tonnage 

district: 3 

massive 

sulphide 

deposits, 13 

barite 

deposits 

Pb/Zn Zn> Pb Zn>> Pb Tom and 

Jason: 

Pb≥Zn, > 

1on/T Ag. 

SEDEX 

Features 

Presence of 

volc./intr. 

rocks 

Associated 

with facies 

change; 

diffuse 

stringer zone 

textures 

masked by 

metamorphis 

m; neither 

vent facies 

nor breccia. 

Mafic volcanic 

rocks and 

related 

intrusions, 

spatially 

related to 

prospective 

contact. 

Finegrained, 

laminated 

sulphidic 

ores in 

anoxic 

chertlimestoneshale 

basin; 

synsedimenta 

ry 

deformatio 

n; no 

evident 

growth 

fault (only 

slumping 

and 

thickening 

of strata). 

Boundary Ck: 

Zn> Pb 

Associated 

with active 

rifting: coarse 

clastics, 

syndeposition 

al faults, 

brecciated 

vent 

complexes, 

laminated 

ores, 

diamictites, 

volcanism. 

shales: 

high 

carbon 

content 

No Mafic flows 

and tuffs, also 

reworked in 

diamictites. 

23/55 

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Zn>Pb> Cu 

VMS 

features: 

mineralizati 

on above 

metavolcani 

c rocks 

(crystal 

tuffs), Cu 

and Au; 

massive to 

layered 

sulphides. 

Felsic lithic, 

crystal ash 

and lapilli 

tuffs and 

flows below 

mineralizati 

on.

Metamorphism Metamorphic 

recrystallizatio 

n obliterate 

primary 

textures. 

Sedimenta 

ry and 

diagenetic 

textures. 

Alteration sericite muscovite, 

illite 

Geochemistry 

Fe-carbonate 

(hydrothermal 

alteration) 

associated 

with 

silicification 

Y 


The Selwyn Basin Map page displays geochemical anomaly maps for an 

extensive suite of elements. Regional stream geochemical data for the area 

have been treated statistically. The database included, and was limited, to all 

samples falling within the outline of Selwyn Basin, as defined on the Selwyn 

Basin Map Page. For each element, different thresholds were chosen by looking 

at the distribution of values and analyzing the departure from the median for 

that element. This permits a finer display of the distribution of the population 

and a more relevant understanding of the significance of anomalies than what 

is usually possible by just looking at the percentiles. See Appendix 4 for the 

statistical results. 

The median value of a population corresponds to the 50th percentile, and 

represents the value of the middle sample for that specific population 

distribution. An element with a narrow range of values will have its maximum 

value at maybe 2 to 3 times the median. Displaying the 98th percentile would 

show the top 2% of that population but it may not be significantly anomalous. 

Elements with a greater range in values may have values up to 20 or 40 times 

the median, a much more significant departure from the middle value of the 

population, therefore much more anomalous. 

The maximum, minimum (minimum detection limit) and median value is listed 

for each element. Values for the 90th, 95th and 98th percentile are included in 

the legend for comparative purposes. It is recommended to carefully read the 

legend for each element (use the toggle legend button, at the left of the 

horizontal toolbar). Statistical analyses were done for Au, Ag, As, Ba, Cd, Co, 

Cu, Hg, Mn, Mo, Ni, Pb, Sb, Sn, U, V, W, and Zn. 

24/55 

Upper 

greenschist 

footwall 

alteration: 

sericite, Fecarbonate, 

local black 

chlorite

Acknowledgements 

Y 


Thanks to Grant Abbott for guidance and supervision on this project; to Don 

Murphy, Lee Pigage, Roger Hulstein, Robert Stroshein, Dereck Rhodes, Karen 

Pelletier and Leyla Weston for editing selected portions of this document and to 

Gary Stronghill for setting up a great Map Gallery. Alan Daley from Daley 

Networks is responsible for the original web layout. The current layout is by 

David McInnes (YTG). 

25/55

Appendix 1 

Table of formations 

Clastic 

shelf Jurassic 

Jurassic , 

Triassic 

Lower schist 

and older Jones Lake 

unconformity 

Permian Takhandit 

Late 

Mississippian 

to Permian Mount Christie 

unconformity 

Mississippian 

to Permian Tischu 

unconformity 

Mississippian 

to Permian 

Keno Hill 

quartzite 

argillite, slate and 

phylllite, 

carbonaceous 

shale , siltstone, 

sandstone 

skeletal limestone, 

chert, sandstone, 

chert-pebble 

conglomerate 

burrowed shale, 

chert, minor 

limestone and 

dolostone 

siliceous 

calcarenite, 

dolomite, minor 

quartzite, limestone, 

shale , chert and 

chert pebble 

conglomerate 

orthoquartzite, 

quartz-arenite, black 

shale, calcareous 

phyllite, sandy 

limestone 

26/55 

Y 

GEOLOGICAL SURVEY

Turbidit 

e Basin 

Off shelf 

Y 


Mississippian Tay 

calcareous siltstone 

and shale, 

crystalline limestone 

unconformity Devonian Natla shale, limestone, chert 

Lower 

Devonian 

to Mid- 

Mississippian 

Earn Group/ 

shale, siltstone, 

thick sandstone and 

Prevost 

chert-conglomerate 

Devonian Funeral 

unconformity 

siliceous shale, 

chert, local chert, 

unconformity 

Lower 

quartzarenite, 

Devonian 

wacke, mudstone 

to Mid- Earn Group/ and conglomerate; 

Mississippian Portrait Lake 

Diachronous, 

conf./unconformable 

contact 

limestone 

Devonian Grizzly Bear 

bioturbated 

Transitional 

(basin to 

shelf) 

Upper Road River Group/ siltstone, locally (Basinal Ordovician 

Silurian Steel 

dolomitic, mudstone 

graptolitic shale, 

facies only) to Devonian Sapper 

Ordovician Road River Group/ chert, limestone, 

to Silurian Duo Lakes 

siltstone 

alkaline basalt flows, 

pillows, breccias, 

hyaloclastite 

breccias, tuffs and 

Cambrian Volcanics 

agglomerates; minor 

to Ordovician (demster) 

rhyolite 

Cambrian Rabbitkettle silty limestone, 

Cambrian Rabbitkettle 

to Ordovician 

nodular limestone, 

siltstone, sandy 

to Ordovician 

27/55 

limestone, shaly 

limestone; Portrait 

Lake equivalent 

Bioclastic, crinoidal 

limestone, Earn Group 

equivalent 

limestone, silty 

limestone; Road River 

equivalent

Lower 

to Middle 

unconformity 

Cambrian Gull Lake 

Late 

Precambrian 

to early 

Cambrian 

Late 

Precambrian 

Hyland Group/ 

Narchilla 

Hyland Group/ 

Yusezyu (base not 

exposed) 

dolostone, quartz 

sandstone 

slate, siltstone, 

locally bioturbated, 

sandstone, 

limestone, 

conglomerate 

variegated shale, 

siltstone, sandstone, 

limestone 

sandstone, grit to 

quartz-pebble 

conglomerate, shale 

and siltstone 

28/55 

Cambrian Rockslide 

Late 

Precambrian 

to Cambrian Vampire 

Y 


limestone, nodular 

siltstone, oolitic 

limestone, silty 

limestone; Gull Lake 

equivalent 

siltstone, fine-grained 

sandstone; Narchilla 

equivalent

Appendix 2 

Deposit Synopsis 

District Name Anvil district 

Deposit name Vangorda 

Minfile no. 105K 055 

Commodities Pb-Zn-Ag-Au 

Deposit type SEDEX 

Mineralogy 

Host rock 

Zoning 

Geometry 

Alteration 

pale yellow sphalerite, galena, 

minor amounts of chalcopyrite, 

and traces of tetrahedrite, 

bournonite and arsenopyrite 

Immediately at base of and 

approximately 50-75m below Mt 

Mye/ Vangorda contact. Basal 

Vangorda carbonaceous phyllite 

very well developed and thick. 

Considered one Anvil cycle: Upper 

orebody (higher grade): mainly 

massive pyrite-pyrrhotite with 

quartz-barite gangue. Pb, Zn, SiO2 

and Ba contents increase toward 

the top of the deposit. Lower part 

of orebody (lower grade): pyritic 

quartzite, enriched in Cu and Au, 

grades downward into siliceous 

phyllite. 

Two main horizons, numerous 

smaller ones. 1000m X 200m X 

25m flat-lying, massive sulphide 

layer. Probably same interval as 

lowest horizon at Grum and 

equivalent to Faro. Overturned. 

Truncated at northwest end. 

Widespread, substantial in hanging 

wall of lower horizon (footwall of 

smaller upper horizons). Strong 

silicification and impregnation by 

pyrite, pyrrhotite and magnetite. 

Reserves Mined out; Original geological 

reserves: 7.1 Mt at 3.4% Pb, 4.3% 

Zn, 48g/t Ag and 0.75g/t Au, using 

a cut-off grade of 4% Pb + Zn; 

open pit reserves of 5.2 Mt of 

29/55 

Y 

GEOLOGICAL SURVEY

Controls 

similar grade material. 

Feeder zone None identified 

Remobilization 

Pathfinder 

Discovery date 1953 


Deposit name Grum 




Mineralogy 

Host rock 

Zoning 

Geometry 

Alteration 

Stratigraphic, orebodies sheared 

and brecciated along fold limbs. On 

short limb of S fold. 

Small scale brecciation, possible 

flowage in baritic facies (hundreds 

of metres). 

prospecting of stream gossan and 

mineralized stream bank outcrop 

sphalerite, galena, pyrite (cp, aspy 

and sulphosalts) (po, mt); massive 

sulphide facies within each of the 

main horizons 

From approx. 50m below Mt Mye/ 

Vangorda contact to 100m above 

it; lowest horizon 30m below main 

graphitic phyllite, another one 

immediately below it, others within 

Vangorda fm. 

Little evidence, possible Anvil cycle 

but many exceptions. Suggested 

Pb increase upwards. Ribbon 

banded graphitic quartzites more 

common than in other deposits. Au 

and Ag correlate with sulphide 

content. 

Three main horizons, each 2000m 

X 1000m X 30m thick. One other 

subsidiary one, others possible. 

Well developed especially below 

main horizon. White mica 

dominant in southwest, chlorite in 

northeast. 

Reserves Proven mineral reserves 16.9 Mt 

(open-pit mineable) t @ 4.9% Zn, 

3% Pb, 47g/tAg. Partially mined 

30/55 

Y 

GEOLOGICAL SURVEY

out. 

Controls folded stratigraphy; offset by faults 

Feeder zone 


Pathfinder gravity 



Deposit name Faro 




Mineralogy 

Host rock 

Zoning 

None defined. Intensely altered 

and mineralized rocks in footwall of 

lowest horizons with weak 

stringers may be related to feeder. 

Brecciation, minor sulphide 

remobilization along fractures, 

cleavages and faults. Possible 

sulphide flowage during D2. 

py, sph, galena, pyrrhotite, 

chalcopyrite, marcasite with patchy 

barite and trace tetrahedrite, 

bournonite, arsenopyrite in 

siliceous gangue, magnetite 

Mt Mye biotite-andalusitemuscovite-schist, 

100 m below 

contact with Vangorda calc-silicate. 

Amphibolite grade. 

Vertical: upper part: massive, 

high-grade and baritic, enriched in 

Pb-Ag-Ba; basal and outer parts: 

lower grade, quartzose and 

variably carbonaceous, enriched in 

Zn; Lateral: northwest part baritic 

facies; central part massive pyritic 

sulphide facies; southeast part 

ribbon-banded graphitic facies. 

Geometry One main horizon containing 

multiple cycles, plus a minor upper 

horizon 10-20m above main 

horizon; 200m long X 1000m wide, 

30-m average thickness; probably 

equivalent to lowest horizon at 

31/55 

Y 

GEOLOGICAL SURVEY

Alteration 

Reserves 

Grum. 

Feeder zone None defined. 


Bleaching and silicification, and 

quartz-muscovite-plagioclase± 

pyrite alteration in both hanging 

wall and footwall; stronger hanging 

wall alteration than in other Anvil 

deposits 

Mined out. Total production was 

56.58 million tonnes @ 5.03% Zn, 

3.34% Pb and 33.93g/t Ag 

Post-metamorphic breccias, 

fracture filling, minor veins 

Pathfinder Gravity survey, Pb-Zn soil anomaly 



Deposit name Swim 




Mineralogy 

Host rock 

pyrite, pyrrhotite, sphalerite, 

galena, minor chalcopyrite and 

trace amounts of tetrahedrite, 

bournonite and arsenopyrite; 

quartz, gypsum and barite gangue 

20 m below Mt Mye/ Vangorda 

contact in uppermost Mt Mye Fm., 

immediately below thick Vangorda 

graphitic phyllite unit; basal 

carbonaceous unit in Vangorda 

very well developed 

Zoning upper baritic portion 

Geometry 

One main horizon, possibly a thin 

footwall horizon. 400m X 300m X 

20m. Probably equivalent to main 

Grum horizon. Deposit truncated 

(offset) by shallow fault. 

Alteration Weakly developed in footwall. 

Reserves 

Geological: indicated mineral 

resource: 4.74Mt @ 4.7% Zn, 

3.8% Pb, 42g/t Ag (using 6% 

combined cut-off). 

32/55 

Y 

GEOLOGICAL SURVEY

Controls Stratigraphic, in hinge of F2 fold; 

Feeder zone 

Few pre D1 and many pre-D2 qtzchl-cp-po 

veinlets in footwall of 

main lens may represent feeder. 

Remobilization Internal brecciation. 

Pathfinder Airborne magnetic survey. 

Discovery date 


Deposit name Dy (Grizzly) 




Mineralogy 

Host rock 

Zoning 

Geometry 

Alteration 

1965 drilling of gravity survey 

anomaly on claims staked on 

airborne magnetic anomaly. 

sphalerite, galena, pyrite and 

minor chalcopyrite 

Poorly defined Mt Mye/ Vangorda 

contact, uppermost horizon within 

Vangorda fm, remainder of 

horizons in Mt Mye fm. 

Anvil cycles, anomalous 

development of carbonate pyritic 

massive sulphides. Galena 

enriched in massive sulphide 

facies, mainly in baritic zone. 

Multilayered (3-5 horizons) deposit 

spanning contact (transition zone). 

2200m X 1800m X 200m. Shallowdipping 

fault below the deposit. 

Two well defined lobes in plan 

view, one of which is zinc-rich and 

the other lead-rich. 

Moderately to well developed, 

generally better in footwall. 

Stronger towards southwest 

margin of deposit. 

Reserves Inferred and indicated mineral 

resource: 21.3 Mt @ 5.54% Pb, 

7.33% Zn, 81.1g/t Ag, 0.87g/t Au 

using 9% combined cut-off grade. 

Mining would be underground. 

33/55 

Y 

GEOLOGICAL SURVEY

Controls Stratigraphic. 

Feeder zone None defined. 

Remobilization Brecciation. 

Additional exploration is required. 

Pathfinder Geological SEDEX model target. 


1976, drilling of stratigraphic 

target along trend of known 

deposits. 

District Name Howard's Pass (map extent) 

Deposit name XY, Anniv 

Minfile no. 105I 012 

Commodities Zn-Pb 


Mineralogy 

Host rock 

Zoning 

Geometry 

Alteration 

Reserves 

Controls Stratiform. 

Active Member: fine-grained, 

laminated sphalerite, pyrite and 

galena, interlayered with limestone 

and chert. 

Early-Mid Silurian laminated 

carbonaceous mudstone and chert 

of Duo Lake Fm (Road River 

Group). 

Pb/Pb+Zn ratios decrease from the 

base upward and laterally, follows 

transition from cherty limestone to 

chert. 

Both XY and Anniv: sheet-like. XY: 

over 17 m thick, explored for 7 km 

strike length. Anniv: 3 zones, 1524 

m long, 335 m wide and up to 45.7 

m thick (average 12.2 m). 

Development of phyllo-silicates 

(muscovite in Active Layer, illitegroup 

clays in rock matrix 

for both XY and Anniv: geological 

:110 Mt @ 5.4% Zn, 2.3% Pb, 

including high-grade core of 8.2 Mt 

@ 10.6% Zn and 5.5% Pb. Anniv: 

indicated resource of 55.4 Mt 

grading 5.3% Zn and 1.8% Pb plus 

values in cadmium and silver; no 

high grade core. 

34/55 

Y 

GEOLOGICAL SURVEY

Feeder zone 


Inferred from slumping and 

thickening of mineralized units. 

Sulphides remobilized along 

fractures. Holocene supergene ore 

downhill from the deposit. 

Discovery date XY: 1972, Anniv: 1973 

District Name Macmillan Pass (map extent) 

Deposit name Tom 

Minfile no. 105O 001 

Commodities Pb, Zn, Ag 


Mineralogy galena, sphalerite, barite, chert 

Host rock 

Zoning 

Geometry 

Alteration 

Reserves 

Controls 

Feeder zone 



Devonian Earn Group, Portrait Lake 

Fm: Mac Pass member and Tom 

sequence 

Lateral and vertical zoning away 

from vent: Pb, Ag, Sb in Vent 

facies; Zn, Hg mostly in the Pink 

facies, and Ba enriched in the Pink 

and Grey facies (more distal). 

3 tabular zones, 2 of them possibly 

on opposite limbs of anticline. 

Tabular to contorted. 

Silicification, replacement by 

pyrrhotite, pyrite and iron 

carbonate. 

Mineable: 9.28 Mt @ 69.4 g/t Ag, 

7.5% Pb and 6.2% Zn (7% 

combined cut-off grade, 15% 

dilution). 

Two grabens flanking horst block, 

contact between submarine fan 

and carbonaceous cherty 

mudstone. 

Brecciated vent complex is 

associated with syndepositional 

fault scarp talus breccia. 

District Name Macmillan Pass 

35/55 

Y 

GEOLOGICAL SURVEY

Deposit name Jason 


Commodities Pb, Zn, Ag, Ba 


Mineralogy 

Host rock 

Zoning 

Geometry 

Alteration 

Reserves 

Controls 

Feeder zone 

Remobilization Brecciation. 


stratiform galena, sphalerite, pyrite 

with barite, Fe-carbonate and chert 

Devonian Earn Group, Portrait Lake 

Fm: shale and coarse turbidites, 

base of Tom Member. 

Hydrothermal facies, Pb/Pb+Zn 

ratios and thickness of sulphide 

lenses and diamictite decrease 

away from syndepositional fault. 

Zoning from massive and 

brecciated vent complex to 

laminated ores. Barite as distal 

facies. 

Two stacked lenses on opposite 

limbs of the Jason syncline about 

20-40 m thick. 

Silicification, siderite veins and 

replacement. 

14.1 Mt @ 7.09% Pb, 6.57% Zn, 

79.9g/t Ag using 8% combined Pb- 

Zn cut-off grade. 

Stratiform, two zones on opposite 

limbs of fold. 

Interbedded with diamictite 

derived from steep syndepositional 

fault. 

District Name Macmillan Pass 

Deposit name Boundary Creek (Nidd) 


Commodities Pb, Zn 

Deposit type SEDEX (epigenetic) 

Mineralogy galena, sphalerite and pyrite 

Host rock Upper Road River and lower Earn 

36/55 

Y 

GEOLOGICAL SURVEY

Zoning 

Group, Portrait Lake Fm, base of the 

Tom Member. 

Fault: strong vertical compositional 

and textural zoning, breccias occur 

at depth. 

Geometry Two separate lenses. 

Alteration 

Intense hydrothermal alteration: 

silicification, interstitial cements, 

replacement and veins of sulphides 

(py, sph and ga), fe-carbonate, 

quartz and minor sericite. 

Reserves Large tonnage low grade. 

Controls Fault. 

Feeder zone 

Discovery 

date 

Fault conduit for volcanism and 

hydrothermal fluids. 

1978 

District Name Marg 

Deposit name Marg 

Minfile no. 106D 001 

Commodities Fe-Zn-Pb-Cu-Ag-Au 

Deposit type VMS 

Mineralogy 

Host rock 

Zoning 

Geometry 

Alteration 

Massive to semi-massive pyrite, 

sphalerite, chalcopyrite, galena, 

tetrahedrite and arsenopyrite in a 

gangue of quartz, ferroan 

carbonate, muscovite and rare 

barite. 

Earn Group, Marg sequence. At 

contact between felsic 

metavolcanic and carbonaceous 

metasedimentary rocks. 

Fe carb-qtz-sericite-py- in footwall. 

Distal: qtz-rich massive pyrite. 

Size and intensity of lithogeochem 

anomalies, and thickness of 

metavolcanic rocks decrease 

downdip. 

Plunging M-fold. Eight parallel 

sulphide lenses, 4 main ones, most 

of resource in upper two. 

Pervasive muscovite and 

carbonate, local black chlorite. 

37/55 

Y 

GEOLOGICAL SURVEY

Reserves 

Controls 

5.5 Mt of 1.76% Cu, 2.46% Pb, 

4.6% Zn, 62.7 g/t Ag and 0.98 g/t 

Au 

Complexly folded stratiform- 

lenses. 

Feeder zone Linear paleo-vent complex. 

Remobilization Folding and shearing. 

Pathfinder Stream geochemical anomaly. 


Appendix 3 

First staked 1965, volcanogenic 

mineralization outlined in 1988. 

Y 


AG AS AS_INA AU AU_INA BA BA_INA CD CO CO_INA 

min 0.1 0.5 0.25 0.5 1 0.01999 25 0.11 1.01 1 

max 8.7 4850 3800 412 805 99999 110000 83.4 429 380 

median 0.1 7 14 1 4 900 1350 0.5 10 12 

90th % 0.69999 30 45 7 12 1940 4600 5 20 24 

95th % 1 52 81.615 16 17 2427.5 6200 8.5 28 32 

98th % 1.5 96.104 170 32.2 30 3410.9 9417.4 13.3 40 47 

38/55

Y 


CU F FE FE_INA HG MN MO MO_INA NI NI_INA 

min 2 10.01 0.01999 0.3 5.01 2.51 1 0.51 1.01 0.51 

max 1220 3923 33.3 34.5 5950 100000 163 1120 1030 1200 

median 29 409 2.39 3.11 69 428 2 3 27 33 

90th % 73 694.3 3.98 5.029 278 1220 8 10 81 120 

95th % 97 846.15 4.7 5.8945 375 1858.85 12 14 125 170 

98th % 136 1194.6 5.7148 7.7816 510 3796.72 20 20 198.16 250 

PB SB SB_INA U U_INA V W W_INA ZN 

min 1 0.11 0.06 0.1 0.26 2.51 1 0.5 6 

max 8090 60 140 133 170 1782 320 200 7990 

median 14 0.8 1.7 4.4 4.6 30 2 1 113 

90th % 28 3.8 6.3 10.1 9.95 90 4 3 446.8 

95th % 37 6.45 9.2 14.5 14 140 8 4 810.9 

98th % 56 9.46 14 21.822 20 305 16 8.58 1350.8 

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GEOLOGICAL SURVEY

The Geological Framework of the Yukon Territory

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