Metallogeny of the Doyon-bousquet-laronde Mining Camp,

Mercier-Langevin, P., Dubé, B., Lafrance, B., Hannington, M., Galley, A., Moorhead, J., and Gosselin, P., 2007, Metallogeny of the Doyon-Bousquet-LaRonde mining camp, Abitibi greenstone belt, Quebec, in Goodfellow, W.D., ed., Mineral Deposits of Canada: A Synthesis of Major Deposit-Types, DistrictMetallogeny, the Evolution of Geological Provinces, and Exploration Methods: Geological Association of Canada, Mineral Deposits Division, SpecialPublication No. 5, p. 673-701.

METALLOGENY OF THE DOYON-BOUSQUET-LARONDE MINING CAMP, ABITIBI GREENSTONE BELT, QUEBEC

PATRICK MERCIER-LANGEVIN1, BENOÎT DUBÉ1, BENOÎT LAFRANCE2, MARK HANNINGTON3, ALAN GALLEY4,JAMES MOORHEAD5, AND PATRICE GOSSELIN1

1. Geological Survey of Canada, 490 rue de la Couronne, Québec, Quebec G1K 9A92. Cogitore Resources, 1300 Saguenay, Rouyn-Noranda, Quebec J9X 7C3

3. Department of Earth Sciences, University of Ottawa, Marion Hall, 140 Louis Pasteur,Ottawa, Ontario K1N 6N54. Geological Survey of Canada, 601 Booth Street, Ottawa, Ontario K1A 0E8

5. Ministère des Ressources naturelles et de la Faune, 400 Lamaque, Val-d’Or, Quebec J9P 3L4Corresponding author’s email: [email protected]

Abstract

The Doyon-Bousquet-LaRonde (DBL) mining camp deposits are hosted by the volcanic and intrusive rocks of the2701-2696 Ma Bousquet Formation located in the upper part of the 2703-2694 Ma Blake River Group in the Abitibigreenstone belt. Since the 1930s, mining has taken place at eight Au ± base metal deposits in the DBL camp for a cumu-lative production, at the end of 2005, of 67 million tonnes (Mt) of ore at 5.67 g/t Au (381 tonnes Au, or 12.3 Moz). Thetotal production, reserves, and estimated resources amount to 133 Mt of ore at 5.23 g/t Au (694 t Au, or 22.3 Moz).

Three main Au±Cu-Zn-Ag deposit types are recognized in the DBL mining camp: 1) Au-rich volcanogenic massivesulphide deposits (LaRonde Penna, Bousquet 2-Dumagami, Bousquet 1, Westwood, Ellison, Warrenmac); 2) epizonal‘intrusion-related’ Au-Cu sulphide-rich vein systems (Doyon); and 3) shear zone-hosted (‘orogenic’) Au-Cu sulphide-rich veins (Mouska, Mic Mac, Mooshla), which share some characteristics with the first two ore types.

The origin of the Au in the DBL camp has been extensively debated in the past and three models have been pro-posed: synvolcanic or syngenetic, multi-stage, and syndeformation. In these models, Au in the volcanogenic massivesulphide (VMS) and sulphide-rich veins of the camp is considered to be 1) a primary component of the hydrothermalfluids at the origin of the VMS (synvolcanic model) and of the epizonal intrusion-related veins, or 2) in part structurallyintroduced within and in part remobilized from massive sulphides into high-strain zones (multi-stage model), or 3) ofmetamorphic origin (syndeformation model). Recent studies of the LaRonde Penna deposit and the Mooshla synvol-canic pluton-hosted vein systems, combined with the geological synthesis and reconstruction of the DBL mining campgeology, have provided further insights into the synvolcanic or syngenetic model for the introduction of the Au, high-lighting the fact that deformation is not a prerequisite for the formation of Au±Cu-Zn-Ag, Doyon-Bousquet-LaRonde-type deposits, as previously thought.

Résumé

Les gisements du camp minier Doyon-Bousquet-LaRonde (DBL) sont encaissés par les roches volcaniques et intru-sives de la Formation de Bousquet (2701-2696 Ma) se retrouvant au sommet du Groupe de Blake River (2703-2694Ma) dans la ceinture de roches vertes de l’Abitibi. Depuis les années 30, huit gisements d’Au ± métaux usuels ont étéexploités pour une production totale, à la fin de 2005, de 67 Mt de minerai à 5,67 g/t Au (381 t Au, ou 12,3 M onces).Le total de la production, des réserves et des ressources estimées est évalué à 133 Mt de minerai à 5,23 g/t Au (694 tAu, ou 22,3 M onces).

Trois principaux types de dépots à Au±Cu-Zn-Ag sont reconnus dans le camp minier DBL: 1) SMV riches en Au(LaRonde Penna, Bousquet 2-Dumagami, Bousquet 1, Westwood, Ellison, Warrenmac), 2) systèmes de veines épi-zonales à Au-Cu riches en sulfures et reliées à une intrusion (Doyon), et 3) veines à Au-Cu riches en sulfures associéesà des cisaillements (“orogéniques”: Mouska, Mic Mac, Mooshla), lesquelles montrent des similitudes avec les deux pre-miers types de dépôts.

L’origine de l’or dans le camp DBL a été amplement débatu par le passé et trois modèles ont été proposés : syn-volcanique ou syngénétique, multiphasé et syn-déformation. Dans ces modèles, l’or dans les SMV et les veines richesen sulfures du camp est considéré soit comme une composante primaire des fluides hydrothermaux à l’origine des SMV(model synvolcanique), soit en partie comme une composante tardive introduite structuralement et possiblement en par-tie remobilisé de sulfures massifs pré-existants dans des couloirs de déformation (modèle multiphasé), ou encorecomme une composante associée aux fluides métamorphiques reliés aux épisodes de déformation régionale (modèlesyn-déformation). Les études récentes du gisement LaRonde Penna et des systèmes de veines reliés au pluton synvol-canique de Mooshla, ainsi que la synthèse géologique du camp DBL ont mis en évidence plusieurs éléments clés sup-portant le modèle synvolcanique ou syngénétique pour l’introduction de l’or, soulignant le fait que la déformation n’estpas un élément déterminant dans la formation de dépôts à Au ± Cu-Zn-Ag de type Doyon-Bousquet-LaRonde tel quesuggéré par le passé.

Introduction and History

The Doyon-Bousquet-LaRonde (DBL) mining camp islocated in the eastern part of the Blake River Group in theSouthern Volcanic Zone of the Archean Abitibi greenstonebelt, between the Cadillac-Larder Lake fault zone to the

south and the Lac Parfouru fault to the north (Fig. 1). A firstphase of prospecting in this area in the 1920s and 1930s ledto the discovery of the Mic Mac and Mooshla Au-Cudeposits, which were mined between 1939 and 1947. Severalother Au and base metal occurrences were also found at or

near surface during this period (e.g. Thompson-Bousquet,Westwood). A period of limited exploration activity fol-lowed from 1940 to about 1970. A second phase of signifi-cant exploration, comprising drilling and geophysics, led tothe discovery and development of the Doyon (Silverstack),Bousquet 1, and Dumagami Au (-Cu) deposits in the late1970s and 80s (Lulin, 1990). Subsequent surface explorationon the mining properties of this area, or underground fromthe existing mines, helped define several satellite lenses andextensions to known ore zones (e.g. Bousquet 2 andMouska). A third major period of underground and surfaceexploration (stripping, drilling, and geophysics) startedabout 1990 and led to the discovery in 1992-1993 of theLaRonde Penna Au-Zn-Cu-Ag volcanogenic massive sul-phide deposit. Since then, aggressive underground explo-ration continued around the LaRonde Penna, Doyon, andMouska mines, as well as on surface elsewhere in the camp.Except for the LaRonde Penna deposit, which extends from800 to more than 3000 m below surface, all the mined orelenses have been discovered from surface or near surfaceexploration around outcrop showings and follow-up drilling,

and by ground geophysics in areas covered by overburden.The LaRonde Penna deposit was found through drilling atdepth from the Dumagami mine, guided by inferred geolog-ical potential.

Since the 1930s, mining has taken place at eight Au ± basemetal deposits in the DBL camp for a cumulative production,at the end of 2005, of 67 million tonnes (Mt) of ore at anaverage grade of 5.67 g/t Au (381 tonnes (t) Au, equivalentto 12.3 Moz Au; Table 1). Significant amounts of Ag andbase metal also have been produced in the camp since 1999from the LaRonde Penna deposit (Table 1). Overall, produc-tion from the DBL camp accounted for 9.9% of the CanadianAu production in 2005 (Table 2), 14.1% of Ag, 1.3% of Cu,and 12.3% of Zn, representing one of the largest miningcamps and Au producing districts in the country. It is themost economically important mining camp in Quebec (Table2) with three mines currently in operation in the camp;LaRonde Penna, Doyon and Mouska (Fig. 1).

The total past production, current reserves, and estimatedresources for the DBL camp amount to 694 t Au, rankingfifth among the Canadian Au districts (Table 3). The camp

P. Mercier-Langevin, B. Dubé, B. Lafrance, M. Hannington, A. Galley, J. Moorhead, and P. Gosselin

674

71

82

67

65

82

8687

70

Malartic Group

Pontiac Group(Metasediments)

Mic Mac

Warrenmac Bousquet 2

Bousquet 1Dumagami

(LaRonde 1)

LaRonde 2Ellison

Mouska

Doyon

Cadillac-Larder Lake Fault

Lac Imau Fault

Cadillac-Larder Lake Fault

Lac Parfouru Fault

Lac Imau Fault

Doyo

nFau

ltBousquet Fault

Westwood

LaRondePenna

Kewagama Group

N

0 1 2 km

Malartic Group(Volcanics)

Mooshla B

Mooshla AQ

UÉB

EC

ON

TAR

IO

Abitibi subprovince, Canada

DBLcamp

NorandaTimmins

2697

2697

2697Legend

Intrusive rocks

Mooshla Intrusion

Proterozoicdiabase dyke

Late stagetrondhjemite-tonalite

Age of volcanic rocks (Ma)

Age of intrusive rocks (Ma)

Maximum age of sedimentaryrocks (Ma)

Mine in production

Closed mineDeposit

High-strainzone

Mineralized lensprojected up-dip

Early and intermediatestagesgabbro-quartz gabbro-tonalite

Piché GroupMafic volcanic andultramafic

Volcanic rocks

Bousquet Formation(Blake River Group)

Hébécourt FormationBasalt-basaltic andesite-local rhyolite

Upper memberdacite-rhyodacite-rhyolite-local basaltic andesiteLower memberbasalt to rhyolite

Sedimentary rocksTimiskaming Group

Kewagama Group

Cadillac Group

Polymictic conglomerate

Wacke-siltstone andargillite

Wacke-siltstone, argillite,local conglomerate andiron formation

87bedding

Bedding withstratigraphic top

Strike and dip ofmain foliation

Lower memberBousquet felsic sills

Projection: UTM NAD 83

26992698

2697

2698<2687

2698

<26892697

<2686

2701

2704

680000mE 682000mE 684000mE 686000mE 688000mE 690000mE 692000mE53

5000

0mN

5348

000m

N53

4600

0mN

5350000mN

5346000mN

5348000mN

FIGURE 1. Location of the Doyon-Bousquet-LaRonde mining camp in the Abitibi greenstone belt (inset map) and simplified geological map of the hostsequence showing the location of the deposits relative to the major faults in the area. Modified from Lafrance et al. (2003a,b) and Dubé et al. (2004). See textfor U-Pb dating references.

Metallogeny of the Doyon-Bousquet-LaRonde Mining Camp, Abitibi Greenstone Belt, Quebec

675

also hosts two of the fifteen largest Canadian Au deposits(Table 4), and LaRonde Penna is the second largest Audeposit of the VMS class after the Horne deposit (Fig. 2) (seealso Dubé et al., 2007a, Galley et al., 2007; Gibson andGalley, 2007).

Although LaRonde Penna is a VMS deposit, its Au con-tent, in grams per tonne, exceeds that of the combined basemetal content in weight percent, and therefore correspondsto the classification proposed by Poulsen et al. (2000) forAu-rich VMS deposits. The main characteristics of Au-richVMS deposits are described in detail in Poulsen andHannington (1996), Hannington et al. (1999), and Dubé et al.(2007a). Numerous other deposits of the DBL camp are alsoconsidered Au-rich VMS deposits: Bousquet 1, Bousquet 2-Dumagami, Westwood, Ellison, and Warrenmac (Table 1 andFig. 2). The cumulative production, reserves, and resourcesof these VMS deposits is 92 Mt of ore at an average grade of5 g/t Au for a total of 462 t of Au (or 14.8 Moz Au). In termsof tonnage, the DBL camp ranks amongst the largestCanadian VMS districts (c.f. Galley et al., 2007) and firstamong the Au-rich VMS districts subtype (Gosselin andDubé, 2005a; Dubé et al., 2007a). Four of the largest Au-richVMS mines presently known in the world are located in theDBL camp (Bousquet 1, Bousquet 2, Dumagami, andLaRonde Penna; Fig. 2), and six of these deposits (DBL

camp deposits, Horne, and Quemont) are found in the BlakeRiver Group in the Abitibi (Fig. 2).

Despite the fact that most of the reserves and estimatedresources in the camp are hosted in VMS deposits, about halfof the Au produced in the camp to date comes from vein-typedeposits (e.g. Doyon, Mouska, Mic Mac, and Mooshla A;Table 1). Vein-type deposits consist of multi-ounce, cen-timetre- to metre-wide, sulphide-rich vein networks, largelytransposed within the regional foliation. As discussed below,most of the vein systems comprising these deposits arethought to be related to volcanism and magmatism but wereclearly strongly affected by the regional deformation events.

Regardless of the type of mineralization, the origin of theAu in the camp has been a source of much controversy in thepast. Many authors proposed a synvolcanic or syngeneticorigin for the Au (e.g. Filion et al., 1977; Valliant andBarnett, 1982; Valliant and Hutchinson, 1982; Valliant et al.,1982, 1983; Bateman, 1985; Stone, 1990, 1991; Tourigny etal., 1993; Teasdale et al., 1996; Gosselin, 1998). However,the intense although heterogeneous deformation (Tourigny etal., 1988; Tourigny and Tremblay, 1997; Belkabir et al.,1998) that has affected all of the deposits (see below) ledsome authors to conclude that at least a portion of the Aupresent in the deposits of the district had been structurallyintroduced and/or remobilized into high-strain zones (multi-

Deposit Year Mt Au Au Ag Cu Zn Mt Au Au Ag Cu Zn Mt Au Au Ag Cu Zn(g/t) (tonnes) (g/t) (%) (%) (g/t) (tonnes) (g/t) (%) (%) (g/t) (tonnes) (g/t) (%) (%)

Au-rich volcanogenic massive sulphide deposits70.074.07.1110.6472.633.753.074.07.110.6472.633.79991-8891imagamuD

LaRonde Penna*(1) 2000-(2005) 12.3 3.53 43.44 53.7 0.28 2.66 46.46 4.51 209.5 42.7 0.34 2.04 58.76 4.31 252.97 45.0 0.33 2.17Bousquet 1 1978-1996 7.45 5.3 39.5 1.82 5.97 10.9 9.27 5.447 50.36

65.052.6641.841.865.052.6641.841.82002-09912 teuqsuoB4.176.552.04.176.552.0nosillE

27.4491.516.87.4491.516.8doowtseW1.543.01.543.0camnerraW

TOTAL 35.22 5.54 195.19 38.0 0.41 1.69 57.48 4.66 266.5 92.7 5.00 461.71Epizonal "intrusion-related" Au-Cu vein systemsDoyon* 1980-(2005) 29.78 5.55 165.14 7.92 5.17 41.0 2.4 37.7 5.47 206.09

TOTAL 29.78 5.55 165.14 7.92 5.17 41.0 37.7 5.47 206.09Shear zone-hosted Au-Cu vein systemsMouska* 1989-(2005) 1.51 11.55 17.45 0.38 14.4 5.5 3.1 1.89 12.13 22.95

43.326.427.043.326.427.07491-2491caM ciM31.066.9250.031.066.9250.00491-9391alhsooM

TOTAL 2.24 9.35 20.93 0.38 14.4 5.5 2.62 10.09 26.42

67.24 5.67 381.26 65.78 4.78 313.0 133.02 5.23 694.23* Active mines

Mt=million tonnesg/t=gram per tonne

(1) Comprises the LaRonde II mine project reserves and resources

TOTAL DBL mining camp

Production Reserves and geological resources Total for each deposit

TABLE 1. Total production, reserves, and geological resources for the Doyon-Bousquet-LaRonde mining camp.

Production in 2005 Au (t) Qc(1) Can(2) Ag (t) Qc(1) Can(2) Cu (t) Qc(1) Can(2) Zn (t) Qc(1) Can(2)

LaRonde Penna 6.8 28.6% 5.7% 150 76.2% 14.1% 7378 18.9% 1.3% 76545 72.8% 12.3%Doyon 3.3 13.9% 2.8%Mouska 1.7 7.1% 1.4%

Total DBL(3) 11.8 49.6% 9.9% 150 76.2% 14.1% 7378 18.9% 1.3% 76545 72.8% 12.3%

(1) Total production, in 2005, for Quebec (23.8 t Au, 197 t Ag, 39090 t Cu, 105136 t Zn) from National Resources Canada, Minerals and Mining statistics

(2) Total Canadian production, in 2005 (119.7 t Au, 1068 t Ag, 570619 t Cu, 623101 t Zn) from National Resources Canada, Minerals and Mining statistics

(3) Total DBL = Total production in 2005 for the Doyon-Bousquet-LaRonde mining camp active mines

TABLE 2. Contribution of the Doyon-Bousquet-LaRonde mining camp mines to the Quebec and Canada production in 2005.

stage model: e.g., Guha et al., 1982; Tourigny et al., 1989a,b;Belkabir and Hubert, 1995; Belkabir et al., 2004), whereasothers proposed an epigenetic (syndeformation) model inwhich the Au was deposited during regional deformation andmetamorphism, and superimposed onto previously formedalteration and sulphide-rich zones (e.g. Marquis et al.,1990a,b,c; Hoy et al., 1990; Savoie et al., 1990; Marquis etal., 1992; Trudel et al., 1992). More recently, ideas about thegenesis of Au-rich VMS deposits have evolved due to animproved understanding of massive sulphide deposits form-ing on the present-day seafloor (e.g. Hannington et al., 2005,and references therein) and within fossil hydrothermal sys-tems (e.g. Sillitoe et al., 1996; Hannington et al., 1999;Huston, 2000). Recent studies of the LaRonde Penna deposit(Dubé et al., 2004, 2007b; Mercier-Langevin, 2005;Mercier-Langevin et al., 2004, 2007a,b; Hannington et al.,2007) and Mooshla-hosted vein systems (Galley and Pilote,2002; Galley et al., 2003; Galley and Lafrance, 2007), andthe geological synthesis and reconstruction of the DBL min-

ing camp geology (Lafrance et al., 2003a), have providedfurther insights into the synvolcanic or syngenetic model forthe introduction of the Au.

Here, we review the main geological characteristics of theDBL mining camp and present the key attributes for eachtype of ore deposit found in this location. The deposit classi-fications proposed are simplified for the purpose of compila-tion, as most of the deposits in the camp comprise variousore types. The descriptions that are presented are meant toillustrate the wide spectrum of ore and alteration styles rec-ognized in the DBL mining camp, in order to draw somegeneral guidelines for exploration applicable in the Abitibisubprovince and perhaps elsewhere in Archean greenstonebelts and possibly younger volcanic sequences. The geolog-ical setting and the Au-rich volcanogenic massive sulphidedeposits sections presented here are taken, in a large part,from Mercier-Langevin et al. (2007a,b,c), Dubé et al.(2007b), and Hannington et al. (2007).


676

Hébécourt FormationBlake River Group maficvolcanic rocksBlake River Group felsicvolcanic rocks

Volcaniclastic rocks

Intrusions

Gabbro

Fault

Data for selected Au-richVMS deposits

14

532

ON

TAR

IO

QU

EB

EC

Rouyn-Noranda

12

11

9

1087

6

Au-Rich VMS Deposits of the WorldNo. Deposit Tonnage (t) Gold (t)

1 Horne 54 300 000 331.12 Quémont 13 924 000 66.03 Bousquet 1 9 264 940 50.44 Bousquet 2-

Dumagami 15 475 827 112.35 LaRonde Penna 58 757 662 253.06 Eskay Creek 3 121 697 118.67 Big Missouri 2 453 924 7.18 Agnico-Eagle 6 928 978 35.99 Montauban 632 774 2.8

10 Boliden 8 300 000 125.311 Hassai 7 176 035 69.912 Mt. Morgan 116 040 700 321.1

Blake River areadeposits 1 to 5

Doyon-Bousquet-LaRondeMining camp

0 10 20 km

N

Noranda Volcanic Centre

FIGURE 2. Location and statistics of a selection of Au-rich VMS deposits of the world with emphasis on the unique concentration of this type of deposit inthe Blake River Group of the Abitibi greenstone belt that comprises five of these deposits. Three of these five deposits are part of the Doyon-Bousquet-LaRonde mining camp. Statistics from Gosselin and Dubé (2005b). Map of the Blake River Group modified from Lamothe et al. (2005). World map modi-fied from Dubé et al. (2007a).


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Geological Setting

The DBL mining camp is an approx-imately 10 km long, east-west-trendingsuccession of volcanic rocks located 45 km east of Rouyn-Noranda (Fig. 1,insert map). The mining camp is situ-ated in the eastern part of the BlakeRiver Group in the Late ArcheanAbitibi greenstone belt of the SuperiorProvince. The Blake River Group isrestricted in this area to a narrow east-west-striking, south-facing homoclinalvolcanic sequence between sedimen-tary rocks of the <2686 Ma (Davis,2002) Kewagama and the <2687 Ma(Lafrance et al., 2005) Cadillac Groups(Lafrance et al., 2003a) (Fig. 1). Rocksof the DBL camp (Bousquet Formation)represent the upper part of the 2703 to2694 Ma Blake River Group (Péloquinet al., 1990; Barrie et al., 1993;Mortensen, 1993; Ayer et al., 2002;Lafrance et al., 2005). This sequencehad previously been divided into sev-eral lithotectonic domains from north tosouth by Tourigny et al. (1988,1989a,b). Lafrance et al. (2003a) laterformally divided the sequence into theHébécourt Formation in the north andthe Bousquet Formation in the south.

Hébécourt FormationThe Hébécourt Formation comprises

laterally extensive tholeiitic basalt andbasaltic andesite flows, cogenetic gab-broic sills, and small isolated tholeiiticrhyolite flows (Fig. 1). The mafic tointermediate flows are massive to pil-lowed (Fig. 3A) and some are charac-teristically magnetic (Lafrance et al.,2003a; Belkabir et al., 2004). The pil-lows, up to 2.5 m in diameter, are locally variolitic and glom-eroporphyritic. The flows are intercalated with tholeiiticmicrogabbro sills of up to a few tens of metres in thickness.The tholeiitic rhyolites are concentrated near the Mouskamine and are generally very fine grained and schistose. Thezones 07, 08, and 22 at Mouska and the Mic Mac ore zonesare hosted in the Hébécourt Formation (Fig. 1).

Bousquet Formation The Hébécourt Formation is overlain by the Bousquet

Formation, which hosts most of the known ore zones of thecamp. The Bousquet Formation is further subdivided into twomembers: the lower member (2699-2698 Ma) and the uppermember (2698-2697 Ma, Lafrance et al., 2005; Mercier-Langevin et al., 2007b). The lower member is composed oftholeiitic to transitional (between tholeiitic and calc-alkaline)mafic to felsic strata, whereas the upper member is dominatedby transitional to calc-alkaline, intermediate (basaltic andesiteand andesite) to felsic (dacite, rhyodacite, and rhyolite) rocks(Lafrance et al., 2003a; Mercier-Langevin et al., 2004, 2007a,b).

Lower Member of the Bousquet Formation

The laterally extensive (Fig. 1) mafic to intermediate vol-caniclastic units (scoriaceous tuffs, Fig. 3B) of the lowermember are interpreted to be of possible subaqueous pyro-clastic origin (Stone, 1990; Lafrance et al., 2003a). Theseblock, lapilli, and ash tuffs are stratified and cut by coevaland cogenetic dykes and sills, and also by felsic feeder dykesrelated to overlying felsic volcanic rocks of the upper mem-ber (Mercier-Langevin, 2005). In the Doyon area (Fig. 1),this tuffaceous sequence is overlain by a glomeroporphyriticlobe-hyaloclastite dacitic flow dated at 2698.3 ± 0.9 Ma(Lafrance et al., 2005) and by a dacitic to rhyolitic flow brec-cia (Savoie et al., 1991). Elsewhere in the camp, the tuffa-ceous sequence is overlain by a heterogeneous unit (Fig. 1)composed of pillowed basalt and/or andesite that is interca-lated or grades laterally into brecciated flows. The heteroge-neous unit is overlain in the Warrenmac area (Fig. 1) by astrongly altered and deformed rhyodacite (Lafrance et al.,2003a). Tholeiitic to transitional, rhyolitic, blue quartz-bearing sills (Fig. 3C) intruded the interface between the

District Location Number ofdeposits Tonnage Au grade Au (t) rank

(Mt) (g/t) (tonnes)Timmins ON 20 436.7 4.93 2151.4 1Red Lake ON 9 59.8 16.52 987.9 2Kirkland Lake ON 8 67.7 12.81 867.4 3Val d'Or QC 18 180.2 4.50 810.5 4DBL camp QC 7 132.7 5.23 694.2 5Rouyn-Noranda QC 17 101.5 5.78 586.1 6Yellowknife NT 2 28.2 15.94 449.4 7Larder Lake ON 3 42.9 9.17 393.3 8Kemess-Toodoggone BC 2 822.7 0.47 375.7 9Malartic QC 5 62.0 4.87 301.9 10BC=British Columbia. NT=Northwerstern Territories. ON=Ontario. QC=QuebecSource: Gosselin and Dubé (2005a)

Total gold(production, reserves, and estimated resources)

TABLE 3. Major Canadian gold districts.

Deposit

Tonnage (t) Au grade Au rank(tonnes) (g/t) (tonnes)

McIntyre-Hollinger-Coniaurum 104,215,929 9.47 987.0 1Campbell Red Lake 37,549,765 21.28 799.2 2Kirkland Lake 53,407,239 14.94 797.7 3

44.12770.6768,119,811olmeH55.805875.4422,004,111emoD

Sigma - Lamaque 90,350,488 4.92 444.4 674.96354.0887,099,128ssemeK

Horne (VMS) 54,300,000 6.10 331.1 8Kerr Addison 35,976,261 9.10 327.4 9LaRonde Penna 58,757,662 4.31 253.0 10

116.94298.2555,284,68ruomaPGiant-Lolor-Supercrest 15,854,675 15.65 248.2 12Tundra, FAT 113,057,000 2.07 233.7 13Doyon 37,703,649 5.47 206.1 14Negus - Nerco Con 12,345,202 16.30 201.3 15Eskay Creek (VMS) 3,121,664 37.99 118.6 21Dumagami-Bousquet 2 15,475,827 7.25 112.3 22Quémont (VMS) 13,924,000 4.74 66.0 39Bousquet 9,264,940 5.44 50.4 52Westwood 8,613,000 5.19 44.7 58Mouska 1,892,771 12.13 23.0 90Source: Gosselin and Dubé (2005a)

Total gold(production, reserves and estimated resources)

TABLE 4. Major Canadian gold deposits.


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A B

C D

E

G

F

H


679

Hébécourt Formation and the base of the lower member ofthe Bousquet Formation (Lafrance et al., 2003a). The thick-est portion of these sills, dated at 2698.6 ± 1.5 Ma (Lafranceet al., 2003a), is located north of the Bousquet 1, Bousquet2, and Dumagami mines (Fig. 1; Dubé et al., 2004).

Upper Member of the Bousquet Formation

The units of the upper member of the Bousquet Formationare characterized by an irregular distribution throughout theDBL mining camp (Lafrance et al., 2003a; Fig. 1), but arethickest in the LaRonde Penna mine area. The lowermostunit of the upper member consists of dacitic to rhyodaciticlobes and flow-breccia deposits (Fig. 3D). This dacitic torhyodacitic flow breccia interval is intercalated withandesitic flows and hyaloclastites, and it is cut by mafic sillsand dykes, as demonstrated in the Bousquet 2-LaRondePenna area (Mercier-Langevin et al., 2007a). The andesiteflows are locally overlain by fine-grained hyaloclastite of thesame composition and thin beds of fine-grained vol-canogenic sedimentary rocks and graphitic argillite. Theintercalation suggests the emplacement of intermittent felsicautoclastic flows and andesitic flows within restricted basinsor depressions where local or intermittent sedimentationoccurred prior to burial by felsic volcanic rocks (Mercier-Langevin et al., 2007a). This andesite-dacite interval is over-lain by rhyodacitic to rhyolitic flow breccia (Fig. 3E) andcoeval rhyolitic domes or cryptodomes mainly developed inthe LaRonde Penna area and in the Ellison-Warrenmac seg-ment (Fig. 1). The rhyodacitic to rhyolitic flow breccia,dated at 2698 ± 1 Ma in the Doyon mine area (Lafrance etal., 2003a), now completely covers consanguineous domesand/or cryptodomes that are dated at 2698.3 ± 0.8 Ma in theLaRonde Penna mine area (Mercier-Langevin et al., 2007a).A subsequent break in volcanic activity is indicated by thedeposition of thin graphitic argillite beds between theLaRonde Penna and Bousquet 2-Dumagami deposits and bythe formation of concomitant Zn-rich massive sulphides(LaRonde Penna 20 North Zn zone) along the same horizonas the argillite (Mercier-Langevin, 2005), above the rhyo-dacitic to rhyolitic flow breccia. The latter unit is in contactwith the Cadillac Group sedimentary rocks in the central partof the camp (Fig. 1) where the upper member is thinner, butelsewhere it is overlain either by a feldspar- and blue quartz-phyric rhyolite (Fig. 3F), a basaltic andesite, or an autoclas-tic rhyolite (Fig. 1). The latter is the uppermost unit of theupper member of the Bousquet Formation and hosts thefeldspar- and blue quartz-phyric rhyolite and the basalticandesite. The feldspar- and blue quartz-phyric rhyolite wasemplaced, at least in part, as a cryptodome within the upper-most autoclastic rhyolite at 2697.8 ± 1 Ma (Mercier-Langevin et al., 2007a). The basaltic andesite (Fig. 3G)forms a sill and dyke complex that was also emplaced withinthe autoclastic rhyolite, locally cutting through the feldspar-and blue quartz-phyric rhyolite (Fig. 4). The sill and dyke

complex was probably transported through the same struc-tures as the feldspar- and quartz-phyric rhyolite, as suggestedby the close spatial association and the cross-cutting rela-tionships (Fig. 4). They were emplaced more or less syn-chronously with the surrounding autoclastic rhyolite in theupper part of the upper member of the Bousquet Formation.The autoclastic rhyolite is present only in the LaRondePenna mine area and is mostly composed of block- andlapilli-sized flow breccia (Fig. 3H) cut by lobes a few metresin length. Thin layers of crystal tuff are locally intercalatedwith the flow breccia.

Mooshla Pluton The polyphase Mooshla synvolcanic intrusion was

sequentially emplaced into the upper part of the HébécourtFormation and into the overlying lower member of theBousquet Formation (Valliant and Hutchinson, 1982;Gaudreau, 1986; Langshur, 1990; Fig. 1). It hosts theMooshla A and B Au deposits and parts of the Doyon andMouska Au (-Cu) deposits. This intrusive complex wasemplaced as three differentiated intrusive phases: 1) earlytholeiitic to transitional dioritic sills; 2) intermediate tholei-itic to transitional gabbro-tonalite that forms the northernhalf of the intrusion (stages 1 and 2 combined on Fig. 1); and3) late transitional to calc-alkaline trondhjemite and por-phyry, representing the upper part (south) of the intrusion(Galley and Lafrance, 2007). The intermediate phase of gab-bro-tonalite is coeval with the lower member of theBousquet Formation and the later trondhjemitic phase is con-temporaneous and possibly comagmatic with the uppermember (Langshur, 1990; Galley and Lafrance, 2007). Thelate intrusive phase gave a reliable U-Pb zircon age of2696.9 ± 1 Ma (Lafrance et al., 2005). The intermediateintrusive phase gave a more or less reliable age of 2701 ± 1 Ma (Zhang et al., 1993), and an aplitic dyke cutting thisintermediate intrusive phase has been imprecisely dated at2704 ± 4 Ma (Tremblay et al., 1995).

The Mooshla pluton is associated with a series ofhydrothermal events responsible for the formation of thenumerous ore zones that comprise the Mouska, Mooshla Aand B, Mic Mac, and Doyon orebodies. These various stylesof mineralization are representative of synvolcanic and pre-intrusion VMS-style mineralization (Mic Mac), late ‘earlyintrusive’-stage VMS and sulphide-rich vein-type mineral-ization (Mouska), syn ‘late-intrusive’- stage quartz and sul-phide vein-type mineralization (Doyon and Mooshla A), andpost-intrusion or syndeformation quartz ± tourmaline-car-bonate-sulphide vein-type mineralization (Mooshla B andMouska; Belkabir et al., 2004; Galley and Lafrance, 2007).

Cadillac GroupThe Bousquet Formation of the Blake River Group is

overlain by the Cadillac Group turbidite units that have been

FIGURE 3. (A) Pillowed basalts of the Hébécourt Formation, northwest of the LaRonde Penna mine. (B) Scoriaceous tuff of the lower member of the BousquetFormation, northeast of the LaRonde Penna mine. (C) Tholeiitic quartz and feldspar porphyritic Bousquet felsic sills of the lower member of the BousquetFormation, emplaced in the upper part of the Hébécourt Formation, north of the LaRonde Penna mine. (D) Upper member of the Bousquet Formation; dacite-rhyodacite lobes emplaced within fine-grained andesitic hyaloclastite, LaRonde Penna mine. (E) Upper member of the Bousquet Formation; rhyodacite-rhy-olite dome/cryptodome with in situ breccia, south of the LaRonde Penna mine. (F) Upper member of the Bousquet Formation; feldspar and blue quartz-phyricrhyolite, LaRonde Penna mine. (G) Upper member of the Bousquet Formation; lower part of the basaltic andesite sills characterized by a glomeroporphyritictexture, east of the LaRonde Penna mine. (H) Rhyodacitic to rhyolitic block and lapilli tuff of the upper felsic unit in the LaRonde Penna mine host sequence,upper member of the Bousquet Formation.


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Level 86

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Alteration facies(upper levels)Cadillac Group

Blake River GroupBousquet FormationUpper member

Upper felsic unit

Fp and Qtz-phyricrhyolite

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Lower member

1-5% garnet

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>10% garnet

Quartz-muscovite facies

Ore zones--

MassiveSemimassive

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Basaltic andesite

(Aluminous zone)Q z-G t-B -M(1-10% garnet)

t r t s facies

B -Q z-G t andstaurolite

t t rfacies

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5347

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N UTM NAD 83 Host Geology Alteration andMineralization

20 North lens NSNS

FIGURE 4. Geological section through the LaRonde Penna deposit showing the distribution of the upper member units of the Bousquet Formation, the zones7 and 6, the 20 North and 20 South lenses, and the distribution-zonation of the principal alteration assemblages developed along the 20 North lens from sur-face to a depth of 2700 m. Modified from Mercier-Langevin et al. (2007a). And = andalusite, Bt = biotite, Ccp = chalcopyrite, Fp = feldspar, Grt = garnet,Ky = kyanite, Ms = muscovite, Py = pyrite. Qtz = quartz.


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described by Dimroth et al. (1982), Lajoie and Ludden(1984), Stone (1990), and Davis (2002). This turbiditicsequence is younger than 2687 Ma (Davis, 2002). The con-tact between the volcanic and sedimentary rocks is notexposed on surface in the LaRonde Penna area but it hasbeen intersected in many drillholes. This contact has beeninterpreted variously as structural (Dumagami fault ofTourigny et al., 1988, 1989b, 1993; Marquis et al., 1990a)and as conformable (Valliant and Hutchinson, 1982; Stone,1990). In the LaRonde Penna mine area, the contact isslightly discordant (i.e. interpreted to be erosional) to sub-concordant as illustrated in section (Fig. 4). A thin horizon(≤20 cm) of semimassive to massive pyrrhotite and pyrite iscommonly present at or near the contact between the vol-canic and sedimentary rocks of the Blake River Group vol-canic sequence and the Cadillac Group sedimentarysequence. It is locally slightly anomalous in Zn (Dubé et al.,2004). This district-wide sulphide-rich interval may resultfrom the interaction between spent or late hydrothermal flu-ids and seawater during a period of nondeposition along theunconformity (Dubé et al., 2007b; Mercier-Langevin et al.,2007a) as the sedimentary rocks were emplaced at least 5 to10 m.y. after cessation of volcanism, as indicated by the ageof the youngest Cadillac Group detrital zircon at LaRondePenna (2689 Ma: Mercier-Langevin et al., 2007a) and atDoyon (2687.4 Ma: Lafrance et al., 2005).

Deformation and MetamorphismThe Blake River Group is characterized by three main

stages of deformation related to north-south convergence,followed by oblique dextral shearing (Dimroth et al., 1983;Hubert et al., 1984). The D1 event caused regional folding(Hubert et al., 1984) and was overprinted by D2, which is themain deformation event in the DBL mining camp (Tourignyet al., 1988; Marquis et al., 1990a, Mercier-Langevin et al.,2004, 2007a). An east-west-trending, steeply south-dippingpenetrative schistosity (regional S2) is present everywhere inthe camp and is responsible for strong flattening, stretching,folding, and shearing of the primary features in mostdeposits (e.g. Bousquet 1: Tourigny et al., 1989b; Bousquet2: Tourigny et al., 1993; Dumagami: Marquis et al., 1990b,c; Doyon: Savoie et al., 1990; 1991). A stretching lineationsteeply plunging west is locally developed on the S2 schis-tosity. A north-northeast-trending cleavage is locally super-imposed on the main schistosity and late sinistral north-northeast-trending faults are locally developed (e.g. Doyonfault: Savoie et al., 1991; Gosselin, 1998). Two episodes ofmetamorphism have been recognized in the region: a pro-grade upper greenschist- to lower amphibolite-facies episodeassociated with the main deformation event D2, and a sub-sequent retrograde greenschist-facies event (Powell et al.,1995). The same metamorphic episodes have been recognized throughout the DBL mining camp (Tourigny etal., 1989a; Marquis et al., 1990a; Lafrance et al., 2003a;Mercier-Langevin, 2005; Dubé et al., 2007b).

Mineral Deposits

Deposit TypesThe classification of the Au ± Cu-Zn-Ag deposits of the

DBL mining camp has evolved with the different interpreta-tions and the continual advancement of knowledge about

lode Au deposits, VMS deposits, and epithermal deposits.The Bousquet 1 deposit and surrounding ore zones wereclassified by Valliant and Hutchinson (1982) as stratiformvolcanic-sedimentary exhalative pyritic bodies and subcon-formable sulphidic veins, whereas the Doyon ore zones wereinterpreted as epigenetic (syndeformation). Epigenetic veins(e.g. Doyon) and epigenetic sulphide-rich zones (e.g.Bousquet 1) were considered by Savoie et al. (1990) and byTrudel et al. (1992) to characterize the mineralization of theBousquet district. The Doyon deposit was later described asporphyry-like by Poulsen (1996), as an intrusion-hosted Ausystem by Poulsen and Hannington (1996) and Hanningtonet al. (1999), and as an intrusion-related Au-Cu sulphide-richvein-type deposit by Poulsen et al. (2000), whereas theBousquet deposit, as well as the Bousquet 2-Dumagami andLaRonde Penna orebodies, were considered to be synvol-canic pyritic Au deposits by Poulsen and Hannington (1996)and Hannington et al. (1999), and submarine Au-rich VMSdeposits by Poulsen et al. (2000). The reader is referred tothese contributions for a discussion of the characteristics ofeach deposit and its proposed classification.

The classification presented here is a simplified schemebased on the descriptions presented in the publications citedabove and on more recent detailed work conducted in thecamp (e.g. Galley and Lafrance, 2007; Dubé et al., 2007b;Hannington et al., 2007; Mercier-Langevin et al., 2007a,b,c).Three main deposit types are recognized in the DBL miningcamp: 1) the Au-rich VMS deposits that comprise theLaRonde Penna lenses, the Bousquet 2-Dumagami orebody,the Bousquet 1 orebody, and the Westwood, Ellison, andWarrenmac ore zones; 2) the epizonal ‘intrusion-related’ Au-Cu vein systems that comprise the Doyon deposit; 3) theshear zone-hosted (‘orogenic’) Au-Cu veins that include theMouska, Mic Mac, and Mooshla A and B deposits. The lat-ter are classified as shear zone-hosted deposits as they occuralmost entirely in major structures related to the mainregional deformation episode (D2). However, they sharesome characteristics with the first two ore types and there-fore could in part consist of transposed and/or remobilizedepizonal intrusion-related Au-Cu vein systems or Au-richvolcanogenic sulphides.

Au-Rich Volcanogenic Massive Sulphide DepositsThe Au-rich VMS deposits of the DBL mining camp (i.e.

LaRonde Penna, Bousquet 2-Dumagami, Bousquet 1,Ellison, Westwood, and Warrenmac) have accounted formore than half of the total tonnage and Au produced in thecamp to the end of 2005, with 195 t of Au extracted from 35 Mt of ore at an average grade of 5.54 g/t Au (Table 1).

The Au-rich VMS deposits consist of stacked ore lenses(or mine zones) at different stratigraphic intervals in theBousquet Formation and represent different episodes of sul-phide precipitation in a long-lived hydrothermal system(Dubé et al., 2007b; Mercier-Langevin et al., 2007a). Therelative position of the ore lenses in each deposit is illus-trated in the schematic stratigraphic columns presented inFigure 5. Overall, the various lenses are located higher in thestratigraphy in the eastern part of the camp (e.g. LaRondePenna mine) than in the western part of the camp (e.g.Warrenmac and Westwood lenses: Fig. 5). All the VMS orezones show the same attitude, with a steeply dipping plunge

to the west (Fig. 6) that represents the primary elongationaxis of the mineralization along inferred, regularly spaced,synvolcanic faults (Mercier-Langevin, 2005, Mercier-Langevin et al., 2007a). This general attitude is mimicked ata smaller scale by the distribution of volcanic units at depth,hydrothermal alteration zonation, and metal zonation withinthe lenses (Mercier-Langevin, 2005).

Mineralization

The VMS mineralization of the DBL mining camp ischaracterized by semimassive to massive sulphide lensesand thin zones of transposed sulphide veins and veinlets,commonly associated with variable amounts of disseminatedsulphides. Individual ore zones or lenses are characterizedby different ore types that are gradational from disseminatedand vein sulphides to semimassive to massive sulphides. Theore zones discussed here are presented in an order that isbased on the stratigraphic level, beginning with the lower-most lenses.

At Bousquet 1, the ore is concentrated in five differentzones (1 to 5, from south to north) with about 80 percent ofthe ore in zone 3, which is located at the interface betweenthe lower and upper members of the Bousquet Formation

(Fig. 7). Tourigny et al. (1989a) divided the ore from thesezones in disseminated-type and vein-type mineralizationwith foliation-parallel veins and foliation-oblique veins. Thefoliation-parallel veins are largely dominant in zone 3 andform centimetre- to metre-thick pinch-and-swell structuresalong the main east-west regional foliation. These veins con-sist of sulphides with lesser amounts of quartz and mus-covite. Pyrite is the main constituent of the sulphides withchalcopyrite and minor amounts of sphalerite, pyrrhotite,galena,bornite, rutile, tellurides (altaite and calaverite), andnative Au (Tourigny et al., 1989a). The foliation-obliqueveins are mainly developed in zones 1, 2, 4, and 5, and con-sist of folded, transposed, and discontinuous stringers thatform zones hundreds of metres long (Tourigny et al., 1989a).They are composed predominantly of pyrite and quartz infelsic host rocks (zones 1 and 2) and of pyrite and carbonatein mafic host rocks (zones 4 and 5), with local concentra-tions of chalcopyrite. The foliation-oblique veins also con-tain trace minerals such as sphalerite, galena, arsenopyrite,pyrrhotite, bornite, magnetite, rutile, gudmundite, stannite,and native Au. The auriferous disseminations are present inzones 3 and 5 within disseminated pyrite (up to 10 vol.%)and trace amounts of chalcopyrite, sphalerite, pyrrhotite, and


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Tholeiitic felsic sills(part of the lower memberof the Bousquet Fm.)


Dacite

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rhyolite

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Bousquetproperty

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Doyonzone 1

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Mooshla B

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Ellison AEllison B

Ellison C

Bousquet 1zones 1 and 2

B-1 zone 4Bousquet 1

zone 3

B-1 zone 5

Bousquet 1zone 6

Bousquet 2-Dumagami

20 Southlens

LaRonde Penna20 North lens

LaRonde Pennazone 6

LaRonde Pennazone 7

FIGURE 5. Simplified stratigraphy of the Doyon-Bousquet-LaRonde mining camp illustrating the stratigraphic setting of the main ore lenses in the Doyon,Bousquet 1 and LaRonde Penna areas. This figure shows the thickening of the upper member of the Bousquet Formation towards the east (LaRonde Pennaarea), the stacking of ore lenses, and the general upward distribution of the VMS lenses towards the east. Modified from Lafrance et al. (2003a), Mercier-Langevin et al. (2007a), and Mercier-Langevin et al. (2007c).


683

rare tellurides, and native Au is present around the vein-typeore (Tourigny et al., 1989a). The mineralization at Ellisonand in zones 3-1 and 3-3 (Fig. 6) can be compared to thevein-type ore of the Bousquet 1 mine, as it forms narrow,transposed stringers of semimassive to massive sulphideveins (pyrite with chalcopyrite±sphalerite and trace amountsof pyrrhotite, galena, electrum, and native Au) as shown onFigure 8A.

At Westwood, west of Bousquet 1 (Fig. 6), two mineral-ized corridors have been defined: the North Corridor and theWestwood Corridor, which are in the same stratigraphicinterval as zones 3, 4, and 5 of the Bousquet 1 mine, andzones A, B, and C at Ellison (Fig. 5) in the upper part of thelower member of the Bousquet Formation (Lei, 2004) or atthe base of the upper member. Both the North and Westwoodcorridors consist of metre-wide auriferous disseminated sul-phide zones cut by centimetre- to decimetre-thick semimas-sive to massive sulphide veins forming transposed stringersin schistose rocks. The disseminated and vein sulphides arelargely dominated by granoblastic pyrite with traces ofpyrrhotite and interstitial chalcopyrite (Fig. 8B). Traceamounts of sphalerite, galena, tellurides, and native Au canbe found in the sulphide veins. This area is characterized bya Au-Cu association, whereas the Warrenmac lens (Figs. 5,6) is characterized by a Au-Zn association (Lei, 2004). TheWarrenmac lens is located near the interface between thelower and upper members of the Bousquet Formation (Fig.5), and consists of semimassive to massive sulphides domi-nated by pyrite with variable amounts of sphalerite, chal-copyrite, and pyrrhotite, and trace amounts of galena, elec-trum, and native Au. Other VMS Zn-Cu anomalies occur atthis stratigraphic interval south-southwest of the Mooshlaintrusion but none contain ore-grade material.

In the eastern part of the camp (Bousquet 2-Dumagami,and LaRonde Penna, Fig. 1), there are many stacked lensesthat mostly sit higher in the stratigraphic sequence than theore zones at Warrenmac, Westwood, Ellison, and Bousquet 1(Fig. 5). The two lowermost ore zones in this area (zones 6and 7 in Figs. 4, 5), located near the base of the upper mem-ber of the Bousquet Formation, consist of semimassive tomassive sulphides that form numerous isolated economiclenses as shown on Figure 6. Some lenses of zones 6 and 7were mined to surface (LaRonde shaft 2) and can be tracedto a depth of more than 2300 m, with zone 7 currently beingmined at depth at LaRonde Penna (Fig. 6). These zones arecomposed of pyrite, chalcopyrite, and sphalerite with minoramounts of pyrrhotite, magnetite, tellurides, and native Au(Hannington et al., 2007). A talus breccia containing Au-richmassive sulphide clasts at the margin of zone 6 was minedclose to surface from shaft 2. This mineralized clast-bearingtalus breccia, developed laterally from the zone 6 massivesulphide mound, probably formed during a volcanism hiatus

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FIGURE 6. Composite longitudinal map (looking north) of the Doyon-Bousquet-LaRonde mining camp ore zones from surface to a depth of 3.2 km. The map excludes the Mouska mine ore zones that are located about2 km west of the Doyon mine. Some ore zones of the Bousquet 1 mine andEllison deposit are not outlined for clarity. The relatively regular spacing ofthe ore lenses is attributed to a major synvolcanic faults system that con-trolled the distribution of the metals and of some volcanic and intrusiveunits through the camp. Modified from Mercier-Langevin et al. (2007c).

in or near local subbasins (Dubé et al., 2007; Mercier-Langevin et al., 2007a). The LaRonde Penna 20 North lensoccurs above zones 6 and 7 in the upper half of the uppermember of the Bousquet Formation (Figs. 4, 5, 6). This lensextends from a depth of 800 m to more than 3200 m (Fig. 6).The lens is currently mined to a depth of 2450 m and it isgoing to be mined to a depth of 3110 m from an internal shaft(LaRonde II mining project: Fig. 6). The 20 North lenslocally reaches more than 40 m in thickness (Fig. 4) and ithas been subdivided into two zones: the 20 North Au zone atthe base (north) and the 20 North Zn zone on top (south) (Fig.4). The 20 North Au zone is composed of auriferous pyriteand chalcopyrite veins and veinlets forming a dense stock-work, with local semimassive centimetre- to metre-thicklenses, which is now strongly flattened and partially trans-posed in the main foliation. This Au-rich stockwork formedby subseafloor replacement in the upper part of a rhyodaciticto rhyolitic flow breccia (Fig. 8C) and represents the feederzone to the 20 North Zn zone massive sulphide lens (Dubé etal., 2007b, Hannington et al., 2007, Mercier-Langevin et al.,2007a). The 20 North Zn zone consists of massive pyrite,sphalerite, and chalcopyrite with minor galena. The spha-lerite is more abundant in the upper part (south) of the 20North Zn zone and forms centimetre- to decimetre-scale

massive bands parallel to the main regional foliation alter-nating with massive pyrite (Fig. 8D). Galena occurs in local-ized, narrow veins and veinlets with sphalerite near the top ofthe lens. A low-grade to barren zone of up to 2 m in thicknessis locally developed between the 20 North Au and the 20North Zn zones. It is composed of coarse pyrite and quartz,and represents the interface between high-temperature min-eralization in the footwall (Au-Cu) and low-temperaturemineralization (Zn-Pb) above (Mercier-Langevin et al.,2004). The 20 North Zn zone also contains dismemberedgraphitic argillite beds that contain nodular pyrite. The pres-ence of sedimentary strata within the Zn-rich part of the lens(upper part) indicates episodes of seafloor exhalative activityat this interface.

At depth in the mine, the 20 North Au zone changes grad-ually into a zone of disseminated to semimassive to locallymassive sulphides (Fig. 8E) composed of auriferous pyriteand chalcopyrite hosted in a quartz, kyanite, andalusite, stau-rolite, and muscovite schist, referred to as the ‘aluminouszone’ (Dubé et al., 2007b; Mercier-Langevin et al., 2007a).The 20 North Zn zone gradually disappears at depth as thealuminous zone develops (Fig. 4). A massive sulphide lenscomposed of auriferous pyrite, chalcopyrite, and sphaleritehas been intersected in the deepest part of the 20 North lens


684

Zone 2

Bousquet 1zone 3

(main zone)

Zone 1

Cadillac Group

Blake River Group

Bousquet Formation

Upper member

Upper felsic unit

Lower member(mafic/intermediate)

Dacite-rhyodacite

N0 50 100 m

Alteration facies

Aluminous alteration(Qtz-And-Ms±Chl-Bt)

Grt-Chl-Cb±Bt-Ms-Qtz-Py(garnetiferous schist)

Qtz-Ms-Py±Chl-Bt(muscovite schist)

>3 g/t Au ore(mostly andalusite schist)<3 g/t Au ore(mostly muscovite schist)

Ore zonesSulphide veins and stringerswith diseminated sulphides

A

A

A

F

F

F

F = fresh, A = altered

687820m

E5347420mNUTM NAD 83

FIGURE 7. Schematic geology of the Bousquet 1 mine area illustrating the distribution of the zones 1, 2, and 3 at the base of the upper member of the BousquetFormation. It also shows the overall distribution of the main alteration assemblages relative to the ore lenses. Modified from Valliant and Barnet (1982),Valliant et al. (1983), and Tourigny et al. (1992). And = andalusite, Bt = biotite, Cb = carbonate, Chl = chlorite, Grt = garnet, Ms = muscovite, Py = pyrite,Qtz = quartz.

FIGURE 8. (A) Narrow, transposed stringers of semimassive to massive sulphide veins of zone 3-1 at Bousquet 1. The stringers are composed of pyrite andchalcopyrite with minor amounts of sphalerite, pyrrhotite, galena, electrum, and native gold in schistose felsic rocks of the upper member of the BousquetFormation typical of Bousquet 1 and Ellison ore zones, East wall. (B) Semimassive sulphide band or vein, which is part of a transposed stringer in theWestwood North corridor. The sulphides consist mainly of granoblastic pyrite with minor amounts of chalcopyrite and pyrrhotite in a quartz-muscovitematrix. (C) Transposed auriferous pyrite and chalcopyrite stringer of the LaRonde Penna 20 North lens (20 North Au zone) emplaced within silicified andsericitized rhyodacitic to rhyolitic flow breccia. (D) Massive sulphides of the LaRonde Penna 20 North lens (20 North Zn zone) composed of pyrite bandsand sphalerite bands. The banding represents the main foliation in the massive sulphides. (E) Disseminated to semimassive sulphides in association with thealuminous alteration developed at depth in the LaRonde Penna mine along the 20 North lens. Ore in the aluminous zone is composed mostly of pyrite andchalcopyrite in a quartz, kyanite, andalusite, and muscovite matrix. (F) Sulphide ore breccia of the Bousquet 2-Dumagami orebody. This ore breccia is com-posed of semimassive to massive pyrite and chalcopyrite supporting silicified wall-rock fragments, West wall. (G) Sulphide ore breccia of the Bousquet 2-Dumagami orebody with interstitial massive bornite±tennantite and tellurides associated with elevated Au and Cu grades. (H) Late north-south fracturescoated with native Au within the Bousquet 2-Dumagami auriferous sulphide zones. And = andalusite, Bn = bornite, Ccp = chalcopyrite, Ky = kyanite, Py =pyrite, Qtz = quartz, Sp = sphalerite.


685

A B

C D

E

G

F

H

and could suggest the development of a second Au-Cu-Zn-Ag zone associated with aluminous alteration at the lowestlevels in the LaRonde Penna mine. A complex assemblage ofaccessory and trace minerals such as arsenopyrite, tetra-hedrite, stannite, magnetite, Bi and Au tellurides, Pb, Sb andAg sulphosalts have been identified in the LaRonde Pennamine ores (Dubé et al., 2004; Hannington et al., 2007). Goldis mostly present as electrum and auriferous tellurides.

The Bousquet 2-Dumagami orebody occurs on the samestratigraphic horizon as the LaRonde Penna 20 North lens.However, the rhyodacitic to rhyolitic flow breccia unit in thefootwall of the 20 North lens thins towards the west and isnot present in the Bousquet 2-Dumagami footwall (Fig. 5).This single orebody was developed as two separate mines(Dumagami, later renamed Donald J. LaRonde, andBousquet 2) as it was bisected by a property boundary (Fig.6). The Au- and Cu-rich orebody or lens is characterized byenrichment of Zn and Pb towards the stratigraphic top

(Marquis et al., 1990a; Tourigny et al., 1993; Teasdale et al.,1996). Three principal sulphide facies were recognized inBousquet 2 by Tourigny et al. (1993) from the base to the topof the lens (north to south: Fig. 9). These facies are 1) stringer ore; 2) massive pyrite and sulphide ore breccia;and 3) banded and brecciated sulphide. The stringer ore iscomposed of 15 to 35 vol.% of partially transposed anasto-mosing veins and veinlets of massive pyrite with minoramounts of chalcopyrite, bornite, and tennantite, and tracesof digenite and sphalerite (Tourigny et al., 1993). Massivepyrite and sulphide ore breccia facies occur in the centralpart of the orebody (Fig. 9) and consist of discontinuousmassive pyrite lenses of up to 5 m thick interfingered withpyrite stringers (30 to 60 vol.%) supporting wall-rock frag-ments (Fig. 8F). In the ore, variable amounts of bornite, chal-copyrite, sphalerite, pyrrhotite, galena, tennantite, and chal-cocite are associated with the pyrite; trace amounts of mag-netite, digenite, mawsonite, renierite, tellurides, and colusite


686

-200 m

-400 m

-600 m

Minelevels2

4

6

8

10

14

-200 m

-400 m

-600 m

Minelevels2

4

6

8

10

Alteration faciesCadillac Group

Blake River GroupBousquet Formation

Upper member

Fp and Qtz-phyricrhyolite

Lower member

Quartz-muscovite facies

Massive andsulphide-Si breccia ore

Stringer andbanded/brecciated ore

Dacite-rhyodacite

Basaltic andesite Aluminous zone(Ky-And-Qtz-Ms-Py-Ccp)

Grt-Chl±Cb-Ms-Bt-Qtz±1-10% Mn-rich garnet

Greywacke

Gabbro/andesiteGrt-Ms-Qtz-Bt±Cb-Chl±1-10% Mn-rich garnet

Ore zones

Ore zones

Bousquet 2-Dumagamimain lens

(zone 1 at Bousquet 2)(zone 5 at Dumagami)

South lenses(Py-Sph-Gn)

Dumagami shaft(Donald J. LaRonde)

Bousquet 2-Dumagamimain lens

South lenses

Dumagami shaft(Donald J. LaRonde)

Host Geology Alteration andMineralization

NSNS

6899

20m

E53

4715

0mN

6899

20m

E53

4735

0mN UTM NAD 83

6899

20m

E53

4715

0mN

6899

20m

E53

4735

0mN UTM NAD 83

FIGURE 9. Simplified geological section through the Bousquet 2-Dumagami orebody showing the distribution of the upper member units of the BousquetFormation, the main lens that was defined as zone 1 at Bousquet 2 and zone 5 at Dumagami, the Au-Zn south lenses, and the distribution-zonation of theprincipal alteration assemblages developed along the main lens. Modified from Marquis et al. (1992). And = andalusite, Bt = biotite, Cb = carbonate, Chl =chlorite, Ccp = chalcopyrite, Fp = feldspar, Gn = galena, Grt = garnet, Ky = kyanite, Ms = muscovite, Py = pyrite, Qtz = quartz, Si = silica, Sp = sphalerite.


687

are also found (Marquis et al., 1990a; Tourigny et al., 1993).In this facies, elevated Au and Cu grades are associated withthe presence of bornite interstitial to the granoblastic pyrite(Fig. 8G). The banded and brecciated sulphide facies, mostlydeveloped in the eastern upper part of the lens (Marquis etal., 1990a, Fig. 9), consist of narrow, strongly transposed,and discontinuous semimassive to massive pyrite and/orsphalerite veins and lenses containing variable amounts ofchalcopyrite, bornite, pyrrhotite, and galena (Marquis et al.,1990a, Mercier-Langevin, 2005). The Bousquet 2-Dumagami orebody is characterized by late north-south frac-tures locally filled with sulphides and coated by native Au(Fig. 8H). This feature, restricted to the Au-rich sulphidezones, was originally attributed to a late introduction of Auin the deposits (syn-brittle deformation) but it has since beenshown that most of the Au associated with base metals in thecamp was part of the synvolcanic hydrothermal systemresponsible for the formation of the VMS lenses (see Dubéet al., 2007b; Hannington et al., 2007; Mercier-Langevin etal., 2007a,b). The formation of Au-coated fractures in mas-sive sulphides is apparently the result of local remobilizationof the Au along fracture planes, as first suggested byTourigny et al. (1993).

The uppermost lens in the DBL mining camp is the 20South lens at LaRonde Penna (Figs. 1, 5, 6). This lens islocated above the 20 North lens (Fig. 4) and generally about10 to 15 m below (north) the Cadillac Group sedimentarystrata. The lens is up to 200 m wide and has a known verti-cal extent of at least 1300 m (Fig. 4), from 900 to 2180 mdepth. The economic mineralization is concentrated mainlyin two zones: 1) at 900 to 1580 m depth; and 2) at 1700 to2180 m depth. The lens is thicker (up to 10 m) in the upperlevels of the mine and gets thinner with increasing depth.The massive sulphide portion of the 20 South lens in theupper part of the mine hosts the highest Au grades (as highas 30 g/t Au with 8% Zn, 0.5% Cu, and more than 250 g/tAg, making it one of the richest zones in the camp: Mercier-Langevin et al., 2004; Dubé et al., 2007b). Elsewhere, themineralized zone consists of centimetre- to metre-wide Au-and Zn-rich massive sulphides. Pyrite, pyrrhotite, sphalerite,chalcopyrite, and galena are the most abundant phases in the20 South lens and are accompanied by minor amounts of tel-lurides and electrum. Sphalerite and galena are concentratedtowards the upper part (south portion) of the lens. The 20South lens is slightly discordant to the ore-hosting lithologi-cal units, suggesting that it was formed, at least in part, byreplacement. Towards the centre of the deposit, the lens ishosted by basaltic andesite, whereas to the east the ore ishosted by the rhyodacitic to rhyolitic flow-breccia units thatare present in both the footwall and hanging wall (Fig. 4).

Hydrothermal Alteration

The Au-rich VMS deposits of the DBL mining camp areassociated with upper greenschist-facies metamorphicassemblages that are derived from synvolcanic hydrothermalalteration of the host volcanic rocks (Dubé et al., 2007b).The hydrothermal alteration is widespread and, owing to thestacking of lenses, hanging-wall alteration commonlymerges with the footwall alteration of the overlying lenses.However, a distinct zonation associated with individuallenses is still preserved.

The mafic rocks of the lower member of the BousquetFormation are chloritized and locally epidote-quartz-mag-netite altered away from the ore zones and around theMooshla pluton. Biotite-rich bands and amphibole-richbands are developed in the footwall of some of the ore lensesthat are located above or hosted in mafic rocks (e.g.Westwood, Bousquet 1, Bousquet 2, and zones 6 and 7 atLaRonde Penna). The biotite-rich bands also containfeldspar and muscovite, whereas the amphibole-rich bandscontain chlorite, feldspar, and tourmaline (Fig. 10A). Anassemblage of plagioclase, chlorite (clinochlore), biotite,carbonate (ankerite), muscovite, quartz, and manganese-richgarnet is present in the mafic rocks underlying the Westwoodand Bousquet 1 ore zones (Fig. 10B; Valliant and Barnett,1982; Elioupoulos, 1983; Tourigny et al., 1989a). The garnetporphyroblasts are more abundant near the centre of thealteration zone, immediately beneath the ore lens, rather thanat the periphery, and the garnets contain up to 25% MnO(e.g. Bousquet 1 zone 3: Valliant and Barnett, 1982).Millimetre-sized Mn-rich garnet is also present in the maficfootwall rocks of the Bousquet 2-Dumagami orebody(Marquis et al., 1990a) and locally in the footwall of zone 7at LaRonde Penna (Dubé et al., 2007b). The relative abun-dance of garnet in the mafic rocks is variable from one lensto another but tends to increase with proximity to the ore,together with the abundance of disseminated pyrrhotite andpyrite. The carbonate alteration (ankerite, calcite, anddolomite) in the mafic rocks is more intense towards theBousquet 1 deposit and is well developed in the footwall andimmediate hanging wall of zone A at Ellison in associationwith light green chlorite (Fig. 10C).

Manganese-rich garnet alteration also occurs within thefootwall felsic rocks at Dumagami (Marquis et al., 1990a,b),and especially at LaRonde Penna in the footwall rhyodacite-rhyolite flow breccia of the 20 North lens (Dubé et al.,2007b; Mercier-Langevin et al., 2007a) where it forms alarge, discordant to distal, semiconformable quartz-biotite-garnet assemblage that grades into a proximal quartz-garnet-biotite-muscovite zone mainly developed in the upper andintermediate levels of the mine (~750-2000 m below surface,Fig. 4) below the Zn-rich part of the lens (Dubé et al.,2007b). The abundance (5-30 vol.%) and size (1-15 mm) ofthe Mn-rich garnet porphyroblasts increase towards the 20North lens, where they occur locally in millimetre- to cen-timetre-wide bands of garnet, epidote, clinozoisite, mus-covite, pyrite, and pyrrhotite (Fig. 10D). The garnet is a Mn-rich Fe-Ca spessartine or almandine with up to 16.3 wt.%MnO (Dubé et al., 2007b). In addition to biotite, quartz andmuscovite, and variable amounts of chlorite, amphibole,pyroxene, clinozoïsite, epidote, and chloritoid occur in thegarnet alteration zone in the footwall of the 20 North lens(Dubé et al., 2007b). This alteration assemblage graduallydisappears with depth in the LaRonde Penna mine as the alu-minous alteration develops (see below), but a similar,although less intense, Mn-rich garnet-bearing alterationassemblage is present in the felsic rocks in the hanging wallof the 20 North lens at depth in the mine (Fig. 4; Dubé et al.,2007b). Otherwise, the hanging-wall alteration of the 20North lens at LaRonde Penna is dominated by muscovite,quartz, and variable amounts of fine-grained biotite in felsicrocks. A distinctive pinkish alteration assemblage also is


688

A B

C D

E

G

F

H


689

developed in a mafic sill and dyke complex located in thehanging wall of LaRonde Penna 20 North lens and in thefootwall of the 20 South lens (Dubé et al. 2007b; Mercier-Langevin et al., 2007a,b). This alteration consists of plagio-clase (albite), hornblende, and chlorite replaced by a fine-grained assemblage of quartz, biotite, rutile-titanite,pyrrhotite, and pyrite with minor amounts of tourmaline, cal-cite, epidote, and muscovite (Fig. 10E; Dubé et al., 2007b).

Parts of Bousquet 1 (Fig. 7), Bousquet 2-Dumagami (Fig.9), and LaRonde Penna 20 North lens (Fig. 4) are associatedat depth with a distinctive proximal aluminous alterationassemblage composed of variable amounts of muscovite,aluminosilicates (kyanite, andalusite, and pyrophyllite), andquartz. At LaRonde Penna, the gradual transition fromquartz-garnet-biotite-muscovite footwall alteration to thealuminous alteration at depth is marked by the replacementof garnet and biotite by staurolite, kyanite, and andalusite,and also by increasing amounts of quartz and pyrite towardsthe core of the aluminous alteration zone (Dubé et al.,2007b). Muscovite (±paragonite) is abundant at the periph-ery of the aluminous zone in association with minor amountsof aluminosilicates (Fig. 10F) but gradually decreases inabundance towards the ore zone where the mineralization ishosted in silica-rich (>95 wt.% SiO2) breccias as at Bousquet2 (Fig. 10G). Silica-rich alteration is also developed atWestwood but is of lesser extent and not associated with sig-nificant amounts of aluminosilicates (Fig. 10H). The alumi-nous alteration developed at Bousquet 1, Bousquet 2-Dumagami, and LaRonde Penna is thought to represent themetamorphosed equivalent of an advanced argillic alterationassemblage caused by leaching of the host rock by acidichydrothermal solutions (Tourigny et al., 1993; Teasdale etal., 1996; Dubé et al., 2007b).

The DBL camp Au-rich VMS lenses are associated withdifferent alteration assemblages that can be of regionalextent or restricted to a single deposit (i.e. focussed versusunfocused fluid flow). The 20 North lens at LaRonde Pennaalso illustrates how a single lens can be associated with anumber of different alteration types and metal associations.These important variations in alteration style and distribu-tion should be considered in any exploration models target-ing Au-rich VMS deposits.

Epizonal ‘Intrusion-Related’ Au-Cu Vein SystemsEpizonal ‘intrusion-related’ Au-Cu veins in the DBL min-

ing camp occur mainly in the Doyon mine but possibly alsoin parts of the Mouska deposit as discussed below. The epi-zonal intrusion-related nomenclature proposed here refers tothe inferred link between the hydrothermal activity responsi-ble for the formation of the sulphide-rich Au-Cu veins and the

emplacement, at shallow depth, of late intrusive phases of theMooshla synvolcanic pluton (see Galley and Lafrance, 2007).

The epizonal intrusion-related Au-Cu vein systems of theDoyon mine (Table 1), and some parts of the Mouska mine,include sulphide-rich (75-80 vol.%) veins and veinlets,pyrrhotite-pyrite-chalcopyrite to pyrite-chalcopyrite dissem-inations, and quartz-sulphide veins (Savoie et al., 1991;Trudel et al.,1992; Belkabir and Hubert, 1995; Gosselin,1998; Galley and Lafrance, 2007). They have been inter-preted as epigenetic (syndeformation) or mesothermal byHoy et al. (1990), Marquis et al. (1990b,c), Savoie et al.(1986, 1990, 1991), as syngenetic or synmagmatic by Filionet al. (1977), Valliant and Hutchinson (1982), Arseneau(1995), and Gosselin (1998), and as remobilized synvolcanicmineralization by Guha et al. (1982), Belkabir and Hubert(1995), Galley et al. (2003), and Galley and Lafrance (2007).

At Doyon, the mineralization is concentrated in three dif-ferent zones (Figs. 11, 12): zones 1 and 2 at the southeasternmargin of the Mooshla pluton, and the West zone within thesoutheastern part of the intrusion. Zones 1 and 2 are hostedby highly altered, schistose felsic ± mafic volcanic rocks inthe upper part of the lower member of the BousquetFormation (Fig. 13), and form slightly discordant orebodies(zone 2, Figs. 12, 13) and intensely transposed vein stock-works in highly schistose rocks (zone 1). The West zone con-sists of steeply west-dipping northwest-southeast, north-south, and north-northeast – south-southwest oriented veins(Fig. 14) that cut a tonalitic part of the intermediate intrusivephase (Fig. 11) of the Mooshla pluton (Gosselin, 1998;Galley and Lafrance, 2007). The West zone is also part of aslightly Au-enriched east-west to west-northwest – east-southeast corridor that traverses the entire intrusion (Fig. 11).

Mineralization

Doyon zone 1 consists of numerous pyrite and quartzveinlets or laminations and contains about 20 vol.% sul-phides. The veinlets vary from a few millimetres to a fewcentimetres in width and can contain more than 70 vol.%pyrite (Savoie et al., 1991). They represent sulphide-richvein networks that have been transposed into discrete east-west deformation zones along the southern margin of theMooshla intrusion (Fig. 15A). Minor amounts of chalcopy-rite, sphalerite, galena, arsenopyrite, and chalcocite are asso-ciated with the pyrite (Guha et al., 1982). Native Au is finelydisseminated and interstitial to pyrite grains. Trace minerals,including auriferous tellurides, are also recognized(calaverite, petzite, and altaite: Guha et al., 1982). Thegangue minerals (<30 vol.%) are mainly quartz with mus-covite, carbonates, and chlorite (Guha et al., 1982; Savoie etal., 1990, 1991).

FIGURE 10. Photographs of representative alteration assemblages related to Au-rich VMS lenses of the DBL mining camp. (A) Biotite, feldspar, and mus-covite-rich bands and amphibole, chlorite, feldspar ± carbonate bands developed in the footwall of the Westwood ore lenses and typical of the other ore lenslocated in the lower member of the Bousquet Formation or just above it such as the Bousquet 1 ore zones and the LaRonde Penna zone 7. (B) Proximal alter-ation assemblage composed of plagioclase, chlorite, biotite, carbonate, muscovite, quartz, and manganese-rich garnet developed in the upper part of the lowermember of the Bousquet Formation in the Westwood-Bousquet 1 area. (C) Carbonate, light-green chlorite, muscovite, and quartz alteration assemblage devel-oped in the Ellison zone A horizon. (D) LaRonde Penna 20 North lens alteration assemblage composed of Mn-rich garnet, biotite, chlorite, epidote, mus-covite, pyrite, and pyrrhotite developed in the upper levels of the mine in association with the Zn-rich part of the deposit (20 North Zn zone). (E) LaRondePenna 20 North lens hanging-wall alteration and 20 South lens footwall alteration. This assemblage, composed of quartz, biotite, rutile-titanite, pyrrhotite,and pyrite with minor amounts of tourmaline, calcite, epidote, and muscovite, is developed in the basaltic andesite located between the 20 North and Southlenses. (F) Quartz-muscovite±aluminosilicate assemblage developed at the margin of the aluminous alteration zones of Bousquet 2-Dumagami (photo) andLaRonde Penna. (G) Silica-rich breccia of the Bousquet 2-Dumagami orebody. This alteration is host of the mineralization and is related to an intense acidleaching of the wallrocks, leaving only silica. (H) Proximal quartz-muscovite alteration at Westwood. And = andalusite, Bt = biotite, Cb = carbonate, Chl =chlorite, Grt = garnet, Hbl = hornblende, Ms = muscovite, Pl = plagioclase, Po = pyrrhotite, Py = pyrite. Qtz = quartz.

Doyon zone 2 and the West zone are characterized by sim-ilar vein types that are discordant to the stratigraphy and theregional foliation (Figs. 12, 14, 15B). These veins, charac-terized by a brecciated texture, vary in thickness from a fewcentimetres to a few decimetres, and contain between 10 and75 vol.% sulphides (Fig. 15C) with quartz, dolomite, andcalcite as the main gangue minerals and chlorite, tourmaline,and rutile as trace constituents (Savoie et al., 1990, 1991).Overall, pyrite is the main sulphide in the veins but chal-copyrite can locally be as abundant as pyrite (Fig. 15D). Thepyrite forms coarse-grained, semimassive to massive aggre-gates within the veins. These aggregates are commonly cutby irregular chalcopyrite veins and veinlets that are restrictedto the quartz and sulphide veins. Chalcopyrite is also presentas micro-inclusions within pyrite crystals (Savoie et al.,1991; Gosselin, 1998). Sulphides other than pyrite and chal-copyrite are relatively rare but include sphalerite, pyrrhotite,galena, arsenopyrite, bornite, and chalcocite, which areclosely associated with the chalcopyrite (Savoie et al., 1991).Native Au is locally abundant in the veins of zone 2 and theWest zone, and is commonly associated with tellurides

(calaverite, tetradymite, tellurobismuthite, petzite, andaltaite: Savoie et al., 1990, 1991; Fig. 15E).


At Doyon, zones 1 and 2, which are hosted mainly in vol-canic rocks, are associated with large discordant to subcon-cordant alteration zones (schists) in which the alterationgradually intensifies towards the veins (Fig. 13). The distalalteration consists of a propylitic assemblage composed ofchlorite, muscovite, carbonate, oligoclase, rutile, and pyritewith minor amounts of garnet, chloritoid, and biotite inmafic rocks, and by an assemblage of quartz, plagioclase,muscovite, rutile, and pyrite, and trace amounts of chloritoidand clinozoisite in felsic rocks (Savoie et al., 1991). Theseassemblages are gradually replaced, towards the veins, byquartz, chlorite, muscovite, rutile, and pyrite schists in maficrocks, and by quartz, muscovite, rutile, and pyrite schists infelsic rocks (Fig. 15F). The proximal alteration that hosts themineralization of zones 1 and 2 is composed of quartz, mus-covite, aluminosilicates, rutile, pyrite, and chlorite, with thechlorite being more abundant in mafic rocks (Fig. 13).


690

AB

C

AB

DEG

I

J

HE

HI

C

D

EGI

F

E

Mouska

Mic Mac

Mooshla B

Mooshla ADoyon

Zones 40,50, 50 south

and 60

Zones 07, 08 and 22

Westzone

Zones 1 and 2Open pit

Doyon

faul

t


Bousquet Formation

Cadillac Group

Kewagama Group

Legend

Intrusive rocks

Mooshla Intrusion

Proterozoicdiabase dyke

Late stagetrondhjemite-tonalite(phases G, H, I, J)

Operating / closed mines

Mineralized lens (projected tosurface)

Early and intermediatestages gabbro-quartzgabbro-tonalite(phases A, B, C, D, E, F)

Volcanic rocks

Bousquet Formation(Blake River Group)

Hébécourt FormationBasalt-basaltic andesite-local rhyolite

Upper memberdacite-rhyodacite-rhyolite-local basaltic andesiteLower memberbasalt to rhyolite

Sedimentary rocksKewagama Group

Cadillac Group

Wacke-siltstone andargillite

Wacke-siltstone, argillite,local conglomerate andiron formation

Bousquet felsic sills

A to F

G to J

Anomalous zones (Au±Cu-Ag-Zn)

N

0 500 m 1 km

Projection: UTM NAD 83

680000mE 682000mE 684000mE53

5000

0mN

5348

000m

N5350000m

N5348000m

N

FIGURE 11. Simplified geological map of the Mooshla synvolcanic intrusion. The Mooshla pluton hosts parts of the mineralizations of the Doyon-Bousquet-LaRonde mining camp: zones 40, 50, 50 south, and 60 at Mouska, Mooshla A and B deposits, and a large part of the West zone at Doyon. From Galley andLafrance (2007).


691

Locally, an assemblage of quartz, aluminosilicates, rutile,and pyrite without micas is developed (aluminous alterationof Savoie et al., 1991). The aluminosilicates consist ofandalusite and kyanite porphyroblasts in part retrograded tokaolinite and pyrophyllite.

In contrast, the veins of the West zone at Doyon are hostedby intrusive rocks that do not exhibit the extensive alterationdeveloped in zones 1 and 2. The alteration is mostly concen-trated in the vein selvages, from a few centimetre to a fewdecimetres from the veins (Savoie et al., 1991), especially inthe more ‘mafic’ phases of the intrusion (Gosselin, 1998).The distal alteration is dominated by chlorite, biotite, andepidote (Fig. 15G), which replace primary ferromagnesianminerals, and by muscovite±carbonate that partially replaceplagioclase. Anhydrite-quartz-pyrite-chalcopyrite veins arepresent at the margin of the Doyon mine mineralization(Savoie et al., 1991; Galley and Lafrance, 2007). The proxi-mal alteration is dominated by muscovite, pyrite, quartz, andcarbonate with minor amounts of chlorite and biotite (Fig.14) and is characterized by the complete destruction of theprimary textures (Fig. 15H). Pyrite can constitute up to 15vol.% of the proximal alteration assemblage (Gosselin,1998), where it is commonly hosted within miarolitic cavi-ties (Galley and Lafrance, 2007).

Shear Zone-Hosted Au-Cu Vein SystemsThe shear zone-hosted (and/or remobilized) Au-Cu vein

systems of the DBL mining camp comprise the Mic Mac,

Mooshla A and B, and parts of the Mouska deposit (Table 1).The Mouska deposit consists of a series of subparallel, sub-vertical east-west to northwest-southeast-trending sulphidesand quartz-sulphides vein systems and associated narrow,high-angle reverse ductile and brittle ductile shear zonessuperimposed on the regional foliation (Belkabir and Hubert,1995; Tourigny and Tremblay, 1997; Belkabir et al., 1998).The deformation is partitioned into high-strain zones thathost the veins, and this deformation may have been respon-sible for remobilization of ore that formed prior to deforma-tion and that resemble the epizonal intrusion-related sul-phide-rich veins (e.g. Belkabir, 1995; Belkabir and Hubert,1995; Belkabir et al., 2004; Galley and Lafrance, 2007).Zones 07, 08, and 22 at Mouska and the Mic Mac deposit arehosted in mafic to intermediate volcanic rocks of theHébécourt Formation north of the Mooshla pluton (Figs. 11,16), and zones 40, 50, 50 south, and 60 at Mouska andMooshla A and B ore zones are hosted in the northern part ofthe intrusion (Fig. 11). A number of subsidiary zones andmineralized structures exist around these principal ore zonesin the intrusion, especially in its western half, south ofMouska and west of Doyon (Fig. 11).

Mineralization

Three main types of mineralization are recognized: 1) stringer zones composed of sulphide veins, veinlets, anddisseminations; 2) quartz-sulphide veins; and 3) quartz-sul-phides ± tourmaline-carbonate-chlorite veins (Belkabir and

Zone 2

West zone

Zone 175

Alteration facies Qtz-Ms-And-Ky-Rt-Py-Chl

Qtz-Ms-Py±Chl-Bt-Rt(” )sericite schist”

Chl-Ms-Cb-Py±Grt-Rt Ore zones

Qtz-sulphide veins,sulphide veinlets, anddisseminated sulphides

Qtz-Pl-Ms-Py±Chl-Bt

Qtz-Chl-And-Ky-Rt-Py-Ms

0 200 m 400 m

N

Blake River Group

Bousquet Formation

Upper member

Rhyodacite

Lower member

Dacite

Dacite-rhyodaciteScoriaceous unit(andesite)

Mooshla pluton

Late stage(undifferentiated)

Heterogeneous unit(mafic/intermediate)

Intermediatestage(undifferentiated)

Doyon

Doy

onfa

ult

AF


AF

AF AFAF

AFAFAF AF

683125m

E

5348410mNUTM NAD 83

FIGURE 12. Simplified geological map of the Doyon deposit showing the distribution of the volcanic and intrusive units of the lower and upper members ofthe Bousquet Formation and of the Mooshla pluton. The map also shows the approximate position of the main ore zones projected to surface and a schematicrepresentation of the main alteration assemblages developed around the ore zones. Modified from Savoie et al. (1991). And = andalusite, Bt = biotite, Cb =carbonate, Chl = chlorite, Grt = garnet, Ky = kyanite, Ms = muscovite, Pl = plagioclase, Py = pyrite, Qtz = quartz, Rt = rutile.

Hubert, 1995; Galley and Lafrance, 2006). These veins typ-ically vary in thickness between a few centimetres to a fewdecimetres (Fig. 17A) and rarely are more than a metre inwidth. The sulphide veins and veinlets (type 1) contain vari-able amounts sulphides in a quartz-dominated matrix. Theveins are also associated with disseminated sulphides andabundant chlorite in the wall rocks. The vein sulphides con-sist mainly of chalcopyrite, pyrrhotite, and pyrite, which areaccompanied by trace amounts of magnetite, ilmenite,hematite, sphalerite, electrum, and tellurides of Au, Ag, Pb,and Bi (Belkabir and Hubert, 1995; Belkabir et al., 2004).The disseminated sulphides and stringers (type 1), commonin zone 22 at Mouska (Fig. 16), are enclosed within perva-sively chlorite-altered and sheared volcanic±intrusive rocksand consist mostly of pyrite (up to 50 vol.%: Belkabir andHubert, 1995; Belkabir et al., 2004) with quartz. The secondvein-type (quartz-sulphide: type 2), common in zones 07, 08,40, and 50 at Mouska (Figs. 11, 16), typically contains lessthan 75 vol.% of sulphides. Quartz in these veins is greyish(Fig. 17A), in contrast to other late, barren to weakly miner-alized white quartz-bearing veins. Pyrrhotite and chalcopy-

rite are dominant (Fig. 17B) and are associated with minoramounts of pyrite and trace amounts of magnetite, ilmenite,electrum, and tellurides of Ag and Pb (Belkabir and Hubert,1995). The type 2 veins resemble the epizonal intrusion-related Au-Cu veins such as those found at Doyon. The thirdvein type (quartz-sulphides ± tourmaline-carbonate-chlorite:type 3) is developed mostly in zones 40 and 50 at Mouska(Belkabir and Hubert, 1995) and at Mooshla B (Fig. 17C;Arseneau, 1995; Gosselin, 1998), and is characterizedlocally by a laminated, crack-and-seal, or banded textures(Galley and Lafrance, 2007). These veins contain much lesssulphide (<20 vol.%, mainly chalcopyrite, pyrrhotite, andpyrite). They form as straight-walled veins both parallel todiscrete east-west shears and as associated subhorizontalveins. The quartz-sulphides ± tourmaline-carbonate-chloriteveins locally follow the margins of dioritic dykes that tran-sect the Mooshla intrusion and its volcanic host rocks (e.g.Mooshla A and B deposits). Gold in these three types of min-eralization occurs as micro-inclusions in sulphides, as freegrains ,or filling late microfractures in quartz and/or sul-phides (Belkabhir et al., 2004). This type of vein shares


692

Open Pit

S NDoyon

-0 m

-100 m

-200 m

-300 m

-400 m

Zone 2

Zone 1

Alteration facies

Blake River Group

Bousquet Formation

Upper member

Rhyodacite

Lower member

Dacite

Dacite-rhyodacite

Qtz-Ms-And-Ky-Rt-Py-Chl

Qtz-Ms-Rt-Py±Cld-Chl-Bt("sericite schist")

Chl-Ms-Cb-Py±Grt-Rt

Ore zones

Scoriaceous unit(andesite)

Mooshla pluton

Intermediatestage(undifferentiated)

Qtz-sulphide veins,sulphide veinlets, anddisseminated sulphides

Qtz-Pl-Ms-Py±Chl-Bt

Qtz-Chl-And-Ky-Rt-Py-Ms

0 100 m 200 m

Heterogeneous unit(mafic/intermediate)


AF

AF

AF

AF

AF

AF

68

40

0m

E

53

47

80

0m

N

68

40

0m

E

53

47

40

0m

N UTM NAD 83

FIGURE 13. Simplified composite geological section through the zones 1 and 2 of the Doyon mine showing the distribution of the volcanic and intrusive unitsof the lower and upper members of the Bousquet Formation and of the Mooshla pluton. The map also shows a schematic representation of the main alterationassemblages developed around the ore zones. Modified from Savoie et al. (1991). And = andalusite, Bt = biotite, Cb = carbonate, Chl = chlorite, Cld = chlo-ritoid, Grt = garnet, Ky = kyanite, Ms = muscovite, Pl = plagioclase, Py = pyrite, Qtz = quartz, Rt = rutile.


693

many analogies with orogenic-style or mesothermal-styleauriferous quartz ± tourmaline-carbonate veins.

The disseminated sulphides and the semimassive to mas-sive sulphides in veins show textures typical of remobiliza-tion and recrystallization, such as annealing and durchbewe-gung breccia textures (Belkabir and Hubert, 1995). The sul-phides locally occur in ribbons thought to represent localtransposition in the regional foliation, and chalcopyrite islocally concentrated in small-scale fold hinges associatedwith late reverse movements. The veins themselves areboudinaged (Fig. 17D) and folded along the main schistos-ity, which is concentrated in the vein selvages and veryweakly developed in the host rocks away from the veins(Fig. 17E).


The Au-Cu vein systems of the Mouska, Mic Mac, andMooshla A and B orebodies (Fig. 11) are associated withmetre-wide alteration haloes around the veins, with moreintense hydrothermal alteration adjacent to the veins. Theshearing spatially associated with the ore zones is generallyconfined to corridors defined by the proximal alterationalong the veins (Fig. 17E, F). Away from the veins, the alter-

ation is mainly characterized by chlorite with subsidiaryamounts of carbonate, epidote, muscovite, and quartz withminor amounts of disseminated sulphides (Belkabir et al.,2004). The carbonate alteration is stronger in mafic volcanicrocks than in intrusive rocks. The transition from distal toproximal alteration envelopes is marked by a gradualdecrease in the abundance of plagioclase, hornblende, epi-dote, actinolite, and chlorite abundances, which are replacedby an assemblage of biotite, quartz, muscovite, disseminatedsulphides, and iron oxides (Fig. 17F).

Genetic and Exploration Models

The Bousquet Formation is interpreted to represent theremnants of a composite volcano, about 10 km in diameter,distal to the larger Noranda Volcanic Complex (Fig. 1), northof Rouyn-Noranda (Lafrance et al., 2003a). The volcanic andintrusive rocks comprise a continuous, differentiated succes-sion generated by partial melting of depleted upper mantleand/or juvenile material (mafic crust). The magmatic activ-ity is thought to have been associated with the progressionfrom depleted upper mantle diapirism and mafic-ultramaficmagma underplating and assimilation, to magmatic differen-tiation (assimilation–fractional crystallization) at mid-crustallevels in subsidiary magma chambers within relatively thick,

706800 mN

6700 mN

6600 mN

2200

mE

2300

mE

2400

mE

2500

mE

2600

mE

2700

mE

55

60

60

North shear zone

South shear zone

50

60

Alteration assemblagesProximal: Ms, Qtz, Py, Chl, Bt, CcDistal: Chl, Qtz, Ep, Cc, Py, Bt“Least-altered”: Pl, Hbl, Chl, Bt, Ep

Distal

“Least-altered”

“Least-altered”

Proximal

Distal

0.2 to >5 m wide

Trace of the main foliation

PyCcp

AuTe

Ore

QtzCb

N

F

F

I

II

F

I

Aphyric to Qtz-phyric trondhjemite(late intrusive stage)Doyon tonalite(intermediate intrusive stage)

Lower member of the Bousquet Fm.

Mined veins

Volcanic rocks

0 200 m 400 m

Doyon mineUnderground grid

FIGURE 14. Simplified geological map of the West zone veins on level 4-0 (230 m depth) at Doyon that illustrates the complex distribution of the veins thatare locally at high angle with the east-west regional foliation. These veins are mostly hosted by the Mooshla synvolcanic intrusion. A schematic illustrationof the alteration assemblages developed in the vein selvages is given in the inset. Modified from Gosselin (1998). Bt = biotite, Cb = carbonate, Cal=calcite,Chl=chlorite, Ccp = chalcopyrite, Ep = epidote, Hbl=hornblende, Ms=muscovite, Pl=plagioclase, Py=pyrite, Qtz=quartz, Te=tellurides.


694

A B

C D

E

G

F

H


695

FIGURE 15. Photographs of representative alteration and ore assemblages related to epizonal “intrusion-related” Au-Cu veins. (A) Highly transposed stock-work of sulphide-quartz veins and veinlets of zone 1 at Doyon. The sulphides consist mostly of pyrite with minor amounts of chalcopyrite, sphalerite, galena,arsenopyrite, chalcocite, and tellurides, East wall. (B) Quartz, pyrite, and chalcopyrite veins of zone 2 at Doyon. The zone 2 and West zone sulphide-richveins are locally discordant to the stratigraphy, at a high angle with the main foliation and partially boudinaged, plane view. (C) Foliation-parallel, centime-tre-wide quartz and sulphide vein of the West zone at Doyon. The veins contain up to 75 vol.% sulphides, mainly pyrite and chalcopyrite, East wall. (D)Intrusion-hosted chalcopyrite-rich vein of the West zone at Doyon. Sulphide-rich veins typical of zone 2 and West zone at Doyon commonly show brecciatedtextures with pyrite and/or chalcopyrite isolating quartz ± carbonate-chlorite fragments, plane view. (E) Native Au and greyish tellurides in a quartz-sulphidevein of West zone at Doyon. (F) Proximal alteration assemblage composed of quartz, aluminosilicates, muscovite, rutile, and pyrite that is developed in fel-sic rocks hosting the zones 1 and 2 mineralization at Doyon, East wall. (G) Example of the distal alteration developed in the Mooshla intrusion near the Westzone veins. This alteration is characterized by a gradual replacement of primary ferromagnesian minerals by chlorite, biotite, and epidote and by the partialdestruction of plagioclase by muscovite±carbonate, plane view. (H) Example of the proximal alteration developed in the Mooshla intrusion along the Westzone vein selvages. This alteration is characterized by an assemblage of muscovite, pyrite, quartz, calcite ± chlorite and biotite. Ccp = chalcopyrite, Py =pyrite, Qtz = quartz. Ms = muscovite, Rt = rutile, Te = tellurides.

Zone 07

Zone 08

Zone 22

Mooshla Pluton

-400 m

4800 m

68

02

70

mE

Felsic volcanicrocks

Massive/pillowedandesite

Basalt

Aplite/Dacitedykes

Microdioritedyke

Ore zones07-08-22

Intrusion contact zone

Zones 07 and 08 alteration(Type 2 veins)

Py

Po

Ccp

Ore

0.5 to 5 m wide

Strong shearing

Qtz

Zone 22 alteration(Type 1 veins)

Pro

xim

al

Dis

tal

“L

ea

st-

alt

ere

d”

Pro

xim

al

Dis

tal

“L

ea

st-

alt

ere

d”

Alteration assemblagesProximal: Chl, Qtz, Ep, Mgt, , Ab, CcDistal: Qtz, Ep, Mgt, , Ab, CcLeast-altered: Act-Hbl, Ab, Mgt, Chl, M , Bt

MsBt

s

PyPo

Cp

QtzMgt

ChlMs

BtAb

Ep

Ore

0.5 to 5 m wide

Strong shearing

Zones 40, 50 and 50S alteration(Type 2 veins)

,

(further south in the intrusion)

Pro

xim

al

Dis

tal

“L

ea

st-

alt

ere

d”

Pro

xim

al

Dis

tal

“L

ea

st-

alt

ere

d”

Py

Po

Ccp

Ore

Alteration assemblagesProximal: , Qtz, Chl, Cc, Py, MgtDistal: Qtz, , Ep, Mgt, Bt, Abt, CcLeast-altered: Abt, Chl, Bt, Py, Hbl

BtChl

0.5 to 2 m wide

Shearing

Qtz

Bt

Pro

xim

al

Dis

tal

“L

ea

st-

alt

ere

d”

Pro

xim

al

Dis

tal

“L

ea

st-

alt

ere

d”

Alteration assemblagesProximal: , Chl, Cc, Qtz, Py, MgtDistal: Qtz, Ep, Mgt, Bt, Ab, , CcLeast-altered: Act-Hbl, Ab, Chl, Ms

BtChl

Mouska

68

02

70

mE

53

49

72

5m

N

53

49

92

5m

N

FIGURE 16. Simplified composite geological section through the zones 07, 08, and 22 of the Mouska mine showing the distribution of the volcanic and intru-sive units of the Hébécourt Formation and of the Mooshla pluton. Schematic illustrations of the alteration assemblages developed in the vein selvages is givenin insets for zones 07, 08 (type 2), and 22 (type 1) that are hosted by andesitic to basaltic volcanic rocks of the Hébécourt Formation and for zones 40, 50,and 50 south (type 2) that are hosted by the Mooshla synvolcanic intrusion. Modified from Belkabir and Hubert (1995) and Belkabir et al. (2004). Ab = albite,Act = actinolite, Bt = biotite, Cc = calcite, Chl = chlorite, Ccp = chalcopyrite, Ep = epidote, Hbl = hornblende, Mgt = magnetite, Ms = muscovite, Po =pyrrhotite, Py = pyrite, Qtz= quartz.


696

A B

C D

E F

FIGURE 17. Photographs of representative alteration and ore assemblages related to shear zone-hosted Au-Cu veins. (A) Centimetre- to decimetre-wide, sub-vertical sulphide-rich grey quartz veins hosting the mineralization of zone 50 at the Mouska mine, West wall. (B) Sulphide-rich quartz vein of zone 50 at theMouska mine. The mineralized veins contain up to 75 vol.% sulphides with mainly chalcopyrite and pyrrhotite with minor amounts of pyrite, magnetite,ilmenite, electrum, and tellurides, plane view. (C) Quartz-sulphide ± tourmaline-carbonate-chlorite vein, Mooshla B deposit. (D) Folded and boudinaged sul-phide-rich quartz vein in a narrow shear zone following apparent reverse movement on the shear plane, zone 50, Mouska mine, East wall. (E) A proximal(centimetre- to decimetre-wide) alteration halo is developed along the veins of zone 50 at the Mouska mine. The proximal alteration is composed of a min-eral assemblage dominated by quartz and biotite, with minor amounts of chlorite, calcite, pyrite, and magnetite. The biotite becomes more abundant a fewcentimetres away from the vein selvages (biotite- and quartz-dominated assemblage) and is gradually replaced away from the vein by chlorite (chlorite- andquartz-dominated assemblage). Strain is concentrated in the proximal alteration zone, West wall. (F) Narrow sulphide-rich grey quartz veins of zone 50 atthe Mouska mine associated with a characteristic proximal alteration assemblage that is strongly foliated and composed predominantly of biotite and quartzwith variable amounts of chlorite, calcite, pyrite, and magnetite. The proximal alteration assemblage is restricted to the vein selvages and grades outward afew centimetres to a decimetre to a weakly foliated chlorite-dominated alteration assemblage. Bt = biotite, Cc = calcite, Chl = chlorite, Ccp = chalcopyrite, Mgt = magnetite, Py = pyrite, Po = pyrrhotite, Qtz = quartz.


697

juvenile or immature mafic±felsic crust (see Mercier-Langevin et al., 2007b). This geodynamic context is differ-ent from the extensional back-arc setting proposed for theNoranda Volcanic Complex in the central Blake River Groupwest of the DBL mining camp (Fig. 2) as older and thickercrust is involved in the geodynamic setting and petrogenesisof the DBL volcanic terrain. The inferred setting (i.e. high-pressure felsic volcanic rocks in a rifted volcanic terrain overa relatively thick juvenile lithosphere) is considered to havebeen favourable for the generation of long-lived, deep-seatedhydrothermal fluid circulation, with possible variable contri-butions to the hydrothermal solutions from the crust, fromdegassing magma and from metasomatized upper mantle asdiscussed in Mercier-Langevin et al. (2007b). The felsicrocks generated in this context (dacite, rhyodacite, rhyolite,and intrusive equivalents in the polyphased Mooshla pluton)are transitional to calc-alkaline and correspond to ArcheanFII-type rhyolites, which have been considered to be of lim-ited prospectivity in the literature (Lesher et al., 1986; Hartet al., 2004). The unique concentration of Au-rich VMSdeposits and epizonal intrusion-related Au-Cu vein systemsin association with transitional to calc-alkaline felsic rocks inthe DBL camp demonstrates the elevated prospectivity ofsuch felsic volcanic sequences and also suggests thatArchean FII-type felsic rocks and the inferred geodynamicsetting in which they are produced could be responsible, atleast in part, for the elevated Au content of the associateddeposits and therefore represent favourable exploration tar-gets for primary Au deposits (Mercier-Langevin et al.,2007b).

The upper member of the Bousquet Formation is notablythickened in the LaRonde Penna mine area, which indicatesthe development of a local effusive centre. Such effusivecentres in the camp are probably important sites for the focusof intense hydrothermal activity (Mercier-Langevin et al.,2007a). Despite late deformation and metamorphic events,the locations of synvolcanic faults can be inferred from thedistinct elongation of felsic dome complexes, associatedmafic sill and dyke swarms, and metal zonation within thelenses, especially in the LaRonde Penna and Bousquet 2-Dumagami areas (Mercier-Langevin 2005; Mercier-Langevin et al., 2007a). The distribution of the volcanic unitsand the relatively regular spacing (±500 to 800 m) betweenthe ore lenses at camp scale strongly suggests the systematicdevelopment of synvolcanic faults (e.g. Fig. 6). The sul-phides were deposited locally on the seafloor above thesefaults (e.g. LaRonde Penna 20 North Zn zone) but were alsoformed by concomitant extensive subseafloor replacement(e.g. 20 North Au zone at LaRonde Penna), which explainsthe disseminated, vein type and semimassive nature and dis-tribution of the ore at Bousquet 1, Ellison, and Westwood,for example. This emphasizes the fact that cross-strata per-meability was a key factor in controlling fluid discharge inthis area during protracted volcanism-magmatism andhydrothermal activity. The epizonal intrusion-related Au-Cuveins developed in zone 2 and West zone at Doyon arethought to be related to syn- to late-magmatic faulting of thelate intrusive phases of the Mooshla pluton upon cooling,caused by emplacement at shallow depth (Galley andLafrance, 2007). These volatile-rich late intrusive phasesmay have been responsible for the formation of the aurifer-

ous quartz-sulphide veins and the aluminous alteration asso-ciated with it (Galley and Lafrance, 2007).

The different alteration and mineralization styles devel-oped in the DBL mining camp are best explained by varia-tions along strike in the style of volcanism and magmaticactivity, as exemplified by LaRonde Penna (Fig. 18) (cf.Dubé et al., 2007b; Mercier-Langevin et al., 2007a).Metamorphosed propylitic alteration caused by near-neutral,seawater-dominated hydrothermal fluids in the volcaniclas-tic units in the upper levels of the LaRonde Penna mine andadvanced argillic alteration caused by acidic fluids proximalto shallow felsic subvolcanic intrusions or cryptodomes atgreater depth in the mine coexist along the same mineralizedlens (20 North lens, Fig. 4). A similar situation was proposedfor so-called high-sulphidation deposits formed in the VMSenvironment (Sillitoe et al., 1996). This situation seems tocontrast with subaerial volcanic centres in which near-neu-tral and intensely acidic conditions occur in separate vol-canic-hydrothermal systems unless telescoped (e.g. Sillitoe,1994). These different conditions appear to be possible indifferent parts of the same hydrothermal system in subma-rine environments, in large part due to variable degrees ofmixing between magmatic volatile-rich fluids andhydrothermally convected seawater as shown schematicallyin Figure 18. The model proposed is supported by the grad-ual transition between the two ore styles at LaRonde and bysimilar variations developed at the camp scale (e.g. Au andZn mineralizations at Warrenmac versus Au and Cu zones atWestwood-Ellison-Bousquet 1, with and without intenseacid leaching). Propylitic alteration (i.e. Mn-rich garnet ±quartz, biotite, chlorite, carbonate) commonly represents thedistal footprint of the hydrothermal system at Bousquet 1,Dumagami, and Westwood, but is proximal to the mineral-ization at LaRonde Penna (20 North lens) and Warrenmac.The aluminous alteration (advanced argillic), which isthought to be produced by fluids rich in magmatic volatiles,is a key vector towards Cu-Au ore at depth at LaRonde-Penna or at Bousquet 2-Dumagami and Bousquet 1 (Dubé etal., 2007b). These variations in hydrothermal assemblagesreflect significant variations in the hydrothermal fluidswithin the volcanic complex and correspond to differenttypes of mineralization.

The eruption of the Bousquet Formation upper member,the emplacement of the Mooshla pluton, and the formationof associated precious and base metal deposits at ca. 2698Ma correspond to a particularly fertile episode of Au-richVMS formation in the Blake River Group. This could sug-gest a possible correlation between the petrogenetic evolu-tion of the Abitibi greenstone belt and the Au endowment ofsome deposits (e.g. Mercier-Langevin et al., 2007a).

Although the regional north-south convergence andoblique dextral shearing strongly affected the orebodies,deformation is not a prerequisite for the formation of Au-rich, Doyon-Bousquet-LaRonde-type deposits, as previouslythought. However, the localization of high-strain zones out-side known tectonic corridors, such as major faults, couldindicate the presence of syngenetic alteration zones wheresubsequent deformation was focussed. Deformation can alsobe responsible for the redistribution and possible concentra-tion of Au in narrow structural corridors. As proposed byBelkabir and Hubert (1995), Belkabir et al. (2004), and

Galley and Lafrance (2007), low-grade zones could havebeen ‘upgraded’ around and within the Mooshla pluton.

Specific Objectives of Current and Future Research

A number of challenges remain in developing a practicalmetallogenic model for the Doyon-Bousquet-LaRonde min-ing camp. Specific objectives of current and future researchinclude the following.1. Better constraints on the geological setting and relation-

ships between the various ore zones at the camp scale todefine the main controls on the location and depositionof ore (e.g. in relation to the position of the main syn-volcanic faults). New mapping and 3-D compilationswill improve exploration drilling at depth, as the poten-tial is still very high to find new ore lenses or vein sys-tems.

2. Establish the link between the Mooshla synvolcanicintrusion, its epizonal ‘intrusion-related’ Au-Cu veinsand the surrounding Au-rich VMS deposits and occur-rences in an integrated volcanic, magmatic, andhydrothermal model.

3. Further constrain the timing relationships between vol-canism, plutonism, hydrothermal activity, deformation,and metamorphism using high-precision U-Pb and Re-Os geochronology on volcanic, intrusive, and sedimen-tary rocks as well as on sulphides and graphitic argillitebeds.

4. Trace the hydrothermal upflow zones in the strati-graphic footwall and hanging-wall sequences usingalteration minerals, geochemistry, volcanology, and sta-ble isotope mapping. The stable isotope signature of thevarious alteration zones will also provide insights intothe hydrothermal conditions that prevailed during ore

formation and possibly contribute to answering thequestion about the source(s) of the mineralizing fluids.

5. Characterize the isotopic signature of the Au-rich VMSmineralization and the epizonal ‘intrusion-related’ Au-Cu vein systems versus the shear zone-hosted or remo-bilized Au-Cu vein systems to better constrain thesource(s) of the metals and sulphur.

6. Better understand the origin of the barren sulphideslocated at the contact between the Bousquet Formationvolcanic rocks and the younger Cadillac Group sedi-mentary rocks, and their relationship to productivehydrothermal systems.

7. Document the relationship between the DBL miningcamp and the rest of the Blake River Group, includingother Au-rich VMS (e.g. Horne and Quemont) of theBlake River Group as well as older Au-rich VMSdeposits of the Abitibi greenstone belt.

Acknowledgements

This paper synthesizes more than 30 years of observationsand careful descriptions made by numerous exploration andmining geologists, research scientists, and dedicated stu-dents who had to deal with major tectonic disturbances ofprimary textures and key geological relationships. Thosegeoscientists have to be acknowledged for their efforts andtheir input into the understanding of the DBL mining camp.This mining camp is now one of the major mining areas inCanada, thanks to the mining and exploration companies thatcontinue to believe in the high exploration potential of theAbitibi greenstone belt.

The authors also wish to express their sincere appreciationto Agnico-Eagle Mines Limited and to IAMGOLDCorporation (formerly Cambior Inc.) for their essential sci-


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Degassing(magmaticvolatiles)

Seawater

pp

5.45.3

Upper felsic unit

Dacitic flow breccia

Rhyolite domeVolcaniclastic

rhyolite-rhyodacite

Rhyolite dome and/orcryptodome

20N Zn

20N Au

20N Au “aluminous” ore

20 South lens horizon

Feldspar andquartz-phyric rhyolite

Basaltic andesite

Bo

usq

uet

Fo

rmati

on

up

per

mem

ber

Qtz-Ms-Py-Ccp Ore zones--

MassiveSemimassive

Aluminous zone(Ky-And-Qtz-Ms-Py-Ccp)Qtz-Grt-Bt-Ms±Chl

Fluid flow Synvolcanic faults/conduits

FIGURE 18. Schematic model of the Bousquet 2-LaRonde Penna hydrothermal system. The variations in ore and alteration style observed along the 20 Northlens are illustrated as an example to show the existing alteration styles developed in the Doyon-Bousquet-LaRonde mining camp. These alteration styles canvary from one deposit to another, from one lens to another in a single deposit, or along a single lens as is the case along the 20 North lens at LaRonde Penna.The initiation of the hydrothermal activity responsible for the formation of most of the stacked Au-rich VMS lenses and of the epizonal “intrusion-related”Au-Cu vein systems of the Doyon-Bousquet-LaRonde mining camp is thought to be coincident with a shift in magmatic activity as suggested by the spatialassociation between the mineralizations and the felsic-dominated calc-alkaline volcanic-intrusive rocks of the upper member of the Bousquet Formation andthe late Mooshla intrusive stage. The calc-alkaline felsic volcanism-plutonism of the upper member of the Bousquet Formation marks the gradual magmaticevolution from regional tholeiitic to transitional, mafic-dominated volcanism-plutonism of the Hébécourt Formation and of the lower member of the BousquetFormation. See discussion in the text. Modified from Mercier-Langevin et al. (2007a). And = andalusite, Bt = biotite, Chl = chlorite, Ccp = chalcopyrite, Grt = garnet, Ky = kyanite, Ms = muscovite, Py = pyrite, Qtz = quartz.


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entific contribution, the authorization to publish, and fortheir keen interests in geoscience. M. Boutin and K. Lauzièrecontributed to the drawing of some figures. This paper wassubstantially improved by helpful comments and carefulconstructive reviews by J. H. Bédard, I. R. Jonasson, M.Legault, and the Editor, W. Goodfellow.

Geological Survey of Canada Contribution No. 20060546.

References

Arseneau, G.J., 1995, Metallogeny and Associated Alteration of GoldOccurrences, Bousquet Township, northwestern Quebec: Ph.D. thesis,Colorado School of Mines, Golden, Colorado, 168 p.

Ayer, J., Amelin, Y., Corfu, F., Kamo, S., Ketchum, J., Kwok, K., andTrowell, N., 2002, Evolution of the southern Abitibi greenstone beltbased on U-Pb geochronology: autochthonous volcanic constructionfollowed by plutonism, regional deformation and sedimentation:Precambrian Research, v. 115, p. 63-95.

Barrie, C.T., Ludden, J.N., and Green, T.H., 1993, Geochemistry of volcanicrocks associated with Cu-Zn and Ni-Cu deposits in the Abitibi sub-province: Economic Geology, v. 88, p. 1341-1358.

Bateman, P.W., 1985, Rock Alteration at the Bousquet Gold Mine, Quebec:M.Sc. thesis, University of Western Ontario, London, Ontario, 159 p.

Belkabir, A., 1995, Structure et Métallogénie du Secteur Ouest du DistrictAurifère Archéen de Bousquet, Abitibi, Canada: Ph.D. thesis,Université de Montréal, Montreal, Quebec, 220 p.

Belkabir, A., and Hubert, C., 1995, Geology and structure of a sulfide-richgold deposit: An example from the Mouska gold mine, Bousquet dis-trict, Canada: Economic Geology, v. 90, p. 1064-1079.

Belkabir, A., Hubert, C., and Hoy, L., 1998, Fluid-rock reactions and result-ing change in rheological behaviour of a composite granitoid: theArchean Mooshla stock, Canada: Canadian Journal of Earth Sciences,v. 35, p. 131-146.

——— 2004, Gold emplacement and hydrothermal alteration in metabasicrocks at the Mouska mine, Bousquet district, Abitibi, Quebec, Canada:The Canadian Mineralogist, v. 42, p. 1079-1096.

Davis, D.W., 2002, U-Pb geochronology of Archean metasedimentary rocksin the Pontiac and Abitibi subprovinces, Quebec, constraints on timing,provenance and regional tectonics: Precambrian Research, v. 115, p. 97-117.

Dimroth, E., Imreh, L., Rocheleau, M., and Goulet, N., 1982, Evolution ofthe south-central part of the Archean Abitibi belt, Quebec. Part I:Stratigraphy and paleogeographic model: Canadian Journal of EarthSciences, v. 19, p. 1729-1758.

Dimroth, E., Imreh, L., Goulet, N., and Rocheleau, M., 1983, Evolution ofthe south-central part of the Archean Abitibi belt, Quebec. Part III:Plutonic and metamorphic evolution and geotectonic model: CanadianJournal of Earth Sciences, v. 20, p. 1374-1388.

Dubé, B., Mercier-Langevin, P., Hannington, M., Davis, D., and Lafrance,B., 2004, Le Gisement de Sulfures Massifs Aurifères VolcanogènesLaRonde, Abitibi, Québec: Altérations, Minéralisations et Implicationspour l’ENploration: Ministère des Ressources naturelles, de la Faune etdes Parcs du Québec, MB 2004-03, 112 p.

Dubé, B., Gosselin, P., Mercier-Langevin, P., Hannington, M., and Galley,A., 2007a, Gold-rich volcanogenic massive sulphide deposits, inGoodfellow, W.D., ed., Mineral Deposits of Canada: A synthesis ofMajor Deposit-Types, District Metallogeny, the Evolution ofGeological Provinces, and Exploration Methods: GeologicalAssociation of Canada, Mineral Deposits Division, Special Publication5, p. 75-94.

Dubé, B., Mercier-Langevin, P., Hannington, M.D., Lafrance, B., Gosselin,P., and Gosselin, G., 2007b, The LaRonde Penna world-class Au-richvolcanogenic massive sulfide deposit, Abitibi, Quebec: Mineralogy andgeochemistry of alteration and implications for genesis and explo-ration: Economic Geology, in press.

Elioupoulos, E.G., 1983, Geochemistry and Origin of the Dumagami PyriticGold Deposit, Bousquet Township, Quebec: M.Sc. thesis, University ofWestern Ontario, London, Ontario, 263 p.

Filion, M., Vallée, M., and Lavoie, C., 1977, Les gisements d’or de laSOQUEM-Silverstack, Canton Bousquet, Québec: Canadian Instituteof Mining and Metallurgy Bulletin, v. 70, p.159-172.

Galley, A.G., and Lafrance, B., 2007, Évolution et métallogénie du pluton deMooshla: Ministère des Ressources naturelles et de la Faune, in press.

Galley, A.G., and Pilote, P., 2002, Géologie et métallogénie de l’intrusion deMooshla, district minier de Bousquet, Cadillac, Québec: Ministère desRessources naturelles, DV 2002-10, p. 37.

Galley, A.G., Pilote, P., and Davis, D., 2003, Gold-related subvolcanicMooshla intrusive complex, Bousquet Mining District, P.Q. in OreDeposits at Depth: Challenges and Opportunities: The CanadianInstitute of Mining and Metallurgy, 2003 Field Conference, September23-26, 2003. Technical Sessions Abstract Volume, p. 16.

Galley, A., Hannington, M., and Jonasson, I., 2007, Volcanogenic massivesulphide deposits, in Goodfellow, W.D., ed., Mineral Deposits ofCanada: A synthesis of Major Deposit-types, District Metallogeny, theEvolution of Geological Provinces, and Exploration Methods:Geological Association of Canada, Mineral Deposits Division, SpecialPublication 5, p. 141-161.

Gaudreau, R., 1986, Intrusion Synvolcanique et Minéralisation Aurifère:Exemple du Pluton de Mooshla, Canton de Bousquet, Abitibi: M.Sc.thesis, Université Laval, Quebec, 42 p.

Gibson, H.L., and Galley, A.G., 2007, Volcanogenic massive sulphidedeposits of the Archean Noranda District, Quebec, in Goodfellow,W.D., ed., Mineral Deposits of Canada: A synthesis of Major Deposit-types, District Metallogeny, the Evolution of Geological Provinces, andExploration Methods: Geological Association of Canada, MineralDeposits Division, Special Publication 5, p. 533-552.

Gosselin, G., 1998, Veines de Quartz Aurifères Précoces à la Zone Ouest dela Mine Doyon, Canton de Bousquet, Preissac, Abitibi: M.Sc. thesis,Université du Québec à Chicoutimi, 125 p.

Gosselin, P., and Dubé, B., 2005a, Gold deposits of Canada: Distribution,Geological Parameters and Gold Content: Geological Survey ofCanada, Open-File Report 4896, 1 CD-ROM.

——— 2005b, Gold Deposits of the World: Distribution, GeologicalParameters and Gold Content: Geological Survey of Canada, Open-FileReport 4895, 1 CD-ROM.

Guha, J., Gauthier, A., Vallée, M., Descarreaux, J., and Lange-Brard, F.,1982, Gold mineralization at the Doyon mine (Silverstack), Bousquet,Quebec, in Hodder, R.W., and Petruk, W., eds., Geology of CanadianGold Deposits: Canadian Institute of Mining and Metallurgy, SpecialVolume 24, p. 50-57.

Hannington, M.D., Poulsen, K.H., Thompson, J.F.H., and Sillitoe, R.H.,1999, Volcanogenic gold in the massive sulfide environment: Reviewsin Economic Geology, v. 8, p. 325-356.

Hannington, M.D., de Ronde, C.E.J., and Petersen, S., 2005, Sea-floor tec-tonics and submarine hydrothermal systems: Economic Geology 100thAnniversary Volume, p. 111-141.

Hannington, M.D., Mercier-Langevin, P., Dubé, B., and Gosselin, G., 2007,Mineralogy, geochemistry and isotopic studies of the gold-rich ores ofthe LaRonde Penna deposit: Economic Geology, in prep.

Hart, T.R., Gibson, H.L., and Lesher, C.M., 2004, Trace element geochem-istry and petrogenesis of felsic volcanic rocks associated with vol-canogenic massive Cu-Zn-Pb sulfide deposits: Economic Geology, v. 99, p. 1003-1013.

Hoy, L.D., Trudel, P., Tourigny, G., Kheang, L., Savoir, A., and Crépeau, R.,1990, Isotopic and fluid inclusion constraints on the origin of vein Aumineralization at Bousquet township, Quebec, in Rive, M., Verpaelst,P., Gagnon, Y., Lulin, J.-M., Riverin, G., and Simard, A., eds., TheNorthwestern Quebec Polymetallic Belt: A Summary of 60 Years ofMining Exploration: Canadian Institute of Mining and Metallurgy,Special Volume 43, p. 413-423.

Hubert, C., Trudel, P., and Gélinas, L., 1984, Archean wrench-fault tecton-ics and structural evolution of the Blake River Group, Abitibi belt,Quebec: Canadian Journal of Earth Sciences, v. 21, p. 1024-1032.

Huston, D.L., 2000, Gold in volcanic-hosted massive sulfide deposits: dis-tribution, genesis, and exploration: Reviews in Economic Geology, v. 13, p. 400-426.

Lafrance, B., Moorhead, J., and Davis, D., 2003a, Cadre Géologique duCamp Minier de Doyon-Bousquet-LaRonde: Ministère des RessourcesNaturelles, de la Faune et des Parcs du Québec, ET 2002-07, 43 p.

Lafrance, B., Mercier-Langevin, P., Dubé, B., Galley, A.G., Hannington,M.D., Davis, D.W., Moorhead, J., Pilote, P., and Mueller, W.U., 2003b,Carte Synthèse de la Formation de Bousquet: Partie ouest: Ministèredes Ressources Naturelles, de la Faune et des Parcs; DV 2003-08,échelle 1: 20 000.

Lafrance, B., Davis, D.W., Goutier, J., Moorhead, J., Pilote, P., Mercier-Langevin, P., Dubé, B., Galley, A., and Mueller, W.U., 2005, NouvellesDatations Isotopiques dans la Portion Québécoise du Groupe de BlakeRiver et des Unités Adjacentes: Ministère des Ressources Naturelles, dela Faune et des Parcs du Québec, RP 2005-01, 15 p.

Lajoie, J., and Ludden, J., 1984, Petrology of the Archean Pontiac andKewagama sediments and implications for the stratigraphy of thesouthern Abitibi belt: Canadian Journal of Earth Sciences, v. 21, p. 1305-1314.

Lamothe, D., Harris, J.R., Labbé, J.-Y., Doucet, P., Houle, P., Moorhead, J.,Dion, C., Savard, R., and Melançon, M., 2005, Évaluation du Potentielen Minéralisations de Type Sulfures Massifs Volcanogènes (SMV) pourl’Abitibi: Ministère des Ressources Naturelles, de la Faune et desParcs, EP 2005-01.

Langshur, A., 1990, The Geology, Geochemistry and Structure of theMooshla Intrusion, Bousquet Mining Centre, Quebec: M.Sc. thesis,Université d’Ottawa, 172 p.

Lei, Y., 2004, Secteur Doyon-Mouska: Progression des travaux d’explo-ration et nouvelles découvertes: Ministère des Ressources Naturelles,Faune et Parcs, Québec Exploration 2004, Résumé des Conférences etdes Photoprésentations, p. 12.

Lesher, C.M., Goodwin, A.M., Campbell, I.H., and Gorton, M.P., 1986,Trace-element geochemistry of ore-associated and barren, felsicmetavolcanic rocks in the Superior Province, Canada: Canadian Journalof Earth Sciences, v. 23, p. 222-237.

Lulin, J.-M., 1990, Une analyse du développement minier du nord-ouestquébécois, in Rive, M., Verpaelst, P., Gagnon, Y., Lulin, J.-M., Riverin,G., and Simard, A., eds., The Northwestern Quebec Polymetallic Belt:A summary of 60 Years of Mining Exploration: Canadian Institute ofMining and Metallurgy, Special Volume 43, p. 17-34.

Marquis, P., Brown, A.C., Hubert, C., and Rigg, D.M., 1990a, Progressivealteration associated with auriferous massive sulfide bodies at theDumagami mine, Abitibi greenstone belt, Quebec: Economic Geology,v. 85, p. 746-764.

Marquis, P., Hubert, C., Brown, A.C., 1990b, Gold deposits in deformedmassive sulphide and pyretic alterites in the Bousquet district, southernAbitibi Subprovince, in Ho, S.E., Robert, F., and Groves, D.I. (eds).,Gold and Base-Metal Mineralization in the Abitibi Subprovince,Canada, with Emphasis on the Quebec Segment: University of WesternAustralia, Short Course Notes, Publication No. 24, p. 243-273.

Marquis, P., Hubert, C., Brown, A.C., and Rigg, D.M., 1990c, An evaluationof genetic models for gold deposits of the Bousquet district, Quebec,based on their mineralogic, geochemical, and structural characteristics,in Rive, M., Verpaelst, P., Gagnon, Y., Lulin, J.-M., Riverin, G., andSimard, A., eds., The Northwestern Quebec Polymetallic Belt: ASummary of 60 Years of Mining Exploration: Canadian Institute ofMining and Metallurgy, Special Volume 43, p. 383-399.

Marquis, P., Hubert, C., Brown, A.C., Scherkus, E., Trudel, P., and Hoy,L.D., 1992, Géologie de la Mine Donald J. LaRonde: Ministère del’Énergie et des Ressources du Québec, ET 89-06, 106 p.

Mercier-Langevin, P., 2005, Géologie du Gisement de Sulfures MassifsVolcanogènes Aurifères LaRonde, Abitibi, Québec: Ph.D. thesis,Institut National de la Recherche Scientifique, Eau, Terre etEnvironnement, Université du Québec, Québec, 694 p.

Mercier-Langevin, P., Dubé, B., Hannington, M.D., Davis, D.W., andLafrance, B., 2004, Contexte Géologique et Structural des SulfuresMassifs Volcanogènes Aurifères du Gisement LaRonde, Abitibi:Ministère des Ressources Naturelles, de la Faune et des Parcs duQuébec, ET 2003-03, 47 p.

Mercier-Langevin, P., Dubé, B., Hannington, M.D., Davis, D.W., Lafrance,B., and Gosselin, G., 2007a, The LaRonde Penna Au-rich volcanogenicmassive sulfide deposit, Abitibi greenstone belt, Quebec: Part I.Geology and geochronology: Economic Geology, submitted.

Mercier-Langevin, P., Dubé, B., Hannington, M.D., Richer-Laflèche, M.,and Gosselin, G., 2007b, The LaRonde Penna Au-rich volcanogenicmassive sulfide deposit, Abitibi greenstone belt, Quebec: Part II.Lithogeochemistry and paleotectonic setting: Economic Geology, sub-mitted.

Mercier-Langevin, P., Dubé, B., Lafrance, B., Hannington, M.D., Galley,A., and Moorhead, J., 2007c, A group of papers devoted to the LaRondePenna Au-rich volcanogenic massive sulfide deposit, eastern BlakeRiver Group, Abitibi greenstone belt, Quebec – Preface: EconomicGeology, submitted.

Mortensen, J.K., 1993, U-Pb geochronology of the eastern AbitibiSubprovince. Part 2: Noranda – Kirkland Lake area: Canadian Journalof Earth Sciences, v. 30, p. 29-41.

Péloquin, A.S., Potvin, R., Laflèche, M.R., Verpaelst, P., and Gibson, H.L.,1990, The Blake River Group, Rouyn-Noranda area, Quebec: A strati-graphic synthesis, in Rive, M., Verpaelst, P., Gagnon, Y., Lulin, J.-M.,Riverin, G., and Simard, A., eds., The Northwestern QuebecPolymetallic Belt: A Summary of 60 Years of Mining Exploration:Canadian Institute of Mining and Metallurgy, Special Volume 43, p. 107-118.

Poulsen, K.H., 1996, Lode gold, in Eckstrand, R.O., Sinclair, W.D., andThorpe, R.I., eds., Geology of Canadian Mineral Deposit Types:Geological Survey of Canada, Geology of Canada no. 8, p.323-328.

Poulsen, K.H., and Hannington, M.H., 1996, Volcanic-associated massivesulphide gold, in Eckstrand, R.O., Sinclair, W.D., and Thorpe, R.I.,eds., Geology of Canadian Mineral Deposit Types, Geological Surveyof Canada, Geology of Canada no. 8, p.183-196.

Poulsen, K.H., Robert, F., and Dubé, B., 2000, Geological Classification ofCanadian Gold Deposits: Geological Survey of Canada, Bulletin 540,106 p.

Powell, W.G., Carmichael, D.M., and Hodgson, C.J., 1995, Conditions andtiming of metamorphism in the Southern Abitibi greenstone belt:Canadian Journal of Earth Sciences, v. 32, p. 768-786.

Savoie, A., Perrault, G., and Fillion, G., 1986, Geological setting of theDoyon gold deposit, Bousquet Township, Abitibi, Québec, Canada, inMacDonald, A.J., ed., Proceedings on Gold’86, An InternationalSymposium on the Geology of Gold: Toronto, Ontario, p. 97-107.

Savoie, A., Trudel, P., Sauvé, P., and Perrault, G., 1990, Géologie de la mineDoyon, Cadillac, Québec, in Rive, M., Verpaelst, P., Gagnon, Y., Lulin,J.-M., Riverin, G., and Simard, A., eds., The Northwestern QuebecPolymetallic Belt: A Summary of 60 Years of Mining Exploration:Canadian Institute of Mining and Metallurgy, Special Volume 43, p. 401-411.

Savoie, A., Trudel, P., Sauvé., P., Hoy, L., and Lao, K., 1991, Géologie de laMine Doyon (Région de Cadillac): Ministère des Ressources Naturellesdu Québec, ET 90-05, 80 p.

Sillitoe, R.H., 1994, Erosion and collapse of volcanoes: causes of telescop-ing in intrusion-centered ore deposits: Geology, v. 22, p. 945-948.

Sillitoe, R.H., Hannington, M.D., and Thompson, J.F.H., 1996, High sulfi-dation deposits in the volcanogenic massive sulfide environment:Economic Geology, v. 91, p. 204-212.

Stone, W.E., 1990, Archean volcanism and sedimentation in the Bousquetgold district, Abitibi greenstone belt, Quebec: Implications for stratig-raphy and gold concentration: Geological Society of America Bulletin,v. 102, p. 147-158.

——— 1991, Archean volcanism and sedimentation in the Bousquet golddistrict, Abitibi greenstone belt, Quebec: implications for stratigraphyand gold concentration: Alternative interpretation and reply, Reply:Geological Society of America Bulletin, v. 103, p. 1256-1257.

Teasdale, N., Brown, A., and Tourigny, G., 1996, Gîtologie de la mineBousquet 2: Ministère des Ressources Naturelles, MB 96-37, 43 p.

Tourigny, G., and Tremblay, A., 1997, Origin and incremental evolution ofbrittle/ductile shear zones in granitic rocks: natural examples from thesouthern Abitibi belt, Canada: Journal of Structural Geology, v. 19, p. 15-27.

Tourigny, G., Hubert, C., Brown, A.C., and Crépeau, R., 1988, Structuralgeology of the Blake River at the Bousquet mine, Abitibi, Quebec:Canadian Journal of Earth Sciences, v. 25, p. 581-592.

Tourigny, G., Brown, A.C., Hubert, C., and Crépeau, R., 1989a, Synvolcanicand syntectonic gold mineralization at the Bousquet mine, Abitibigreenstone belt, Quebec: Economic Geology, v. 84, p. 1875-1890.

Tourigny, G., Hubert, C., Brown, A.C., and Crépeau, R., 1989b, Structuralcontrol on gold mineralization at the Bousquet mine, Abitibi, Quebec:Canadian Journal of Earth Sciences, v. 26, p. 157-175.

Tourigny, G., Hubert, C., Brown, A.C., Crépeau, R., Trudel, P., Hoy, L., andKheang, L., 1992, Géologie de la mine Bousquet: Ministère de l’Én-ergie et des Ressources du Québec, ET 89-09, 99 p.

Tourigny, G., Doucet, D., and Bourget, A., 1993, Geology of the Bousquet2 mine: An example of a deformed, gold-bearing polymetallic sulfidedeposit: Economic Geology, v. 88, p. 1578-1597.

Tremblay, A., Tourigny, G., and Machado, N., 1995, Zircon U/Pb age con-straints on deformation and gold mineralization of the Mooshla pluton,


700


701

southern Abitibi belt, Canada: Geological Society of America, AnnualMeeting, New Orleans, Abstract with Programs, p. A-163.

Trudel, P., Sauvé, P., Tourigny, G., Hubert, C., and Hoy, L., 1992, Synthèsedes Caractéristiques Géologiques des Gisements d’Or de la Région deCadillac (Abitibi): Ministère de l’Énergie et des Ressources du Québec:MM 91-01, 106 p.

Valliant, R.I., and Barnett, R.L., 1982, Manganiferous garnet underlying theBousquet gold orebody, Quebec: Metamorphosed manganese sedimentas a guide to gold ore: Canadian Journal of Earth Sciences. v. 19, p. 993-1010.

Valliant, R.I., and Hutchinson, R.W., 1982, Stratigraphic distribution andgenesis of gold deposits, Bousquet region, Northwestern Quebec, inHodder, R.W., and Petruk, W., eds., Geology of Canadian GoldDeposits: Canadian Institute of Mining and Metallurgy, Special Volume24, p. 27-40.

Valliant, R.I., Mongeau, C., and Doucet, R., 1982, The Bousquet pyriticgold deposit, Bousquet region, Quebec: Descriptive geology and pre-liminary interpretations on genesis, in Hodder, R.W., and Petruk, W.,eds., Geology of Canadian Gold Deposits: Canadian Institute of Miningand Metallurgy, Special Volume 24, p. 41-49.

Valliant, R.I., Barnett, R.L., and Hodder, R.W., 1983, Aluminium silicate-bearing rock and its relation to gold mineralization; Bousquet mine,Bousquet Township, Quebec: Canadian Institute of Mining andMetallurgy Bulletin, v. 76, p. 81-90.

Zhang, Q., Machado, N., Ludden, J., and Moore, D., 1993, Geotectonic con-straints from U-Pb ages for the Blake River Group, the KinojévisGroup and the Normétal mine area, Québec: Geological Association ofCanada – Mineralogical Association of Canada, Joint Annual Meeting,Program and Abstracts, v. 18, p. A-114.

Documents

Metallogeny of the Doyon-bousquet-laronde Mining Camp,