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Noranda - Horne, Quemont, Gallen, Amulet, Norbec, Vauze, Ansil, Millenbach, Waite, East Waite, Old Waite, Aldermac, Corbet, Delbridge, F Shaft, Deldona, Mobrun |
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Quebec, Canada |
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Cu Au Zn Ag
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Super Porphyry Cu and Au
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IOCG Deposits - 70 papers
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The Noranda Volcanic Complex within the Abitibi Greenstone Belt of the Superior Province of eastern Canada hosts a cluster of >22 Archaean (2.8 Ga) volcanic hosted massive sulphide deposit within the Rouyn-Noranda district of Quebec, Canada. The complex is believed to be part of a 35 km diameter shield volcano.
The Rouyn-Noranda District is located towards the south-central section of the ~900 x 250 km, ENE-WSW oriented Abitibi Greenstone Belt/Sub-province. This sub-province generally comprises east-trending synformal 'keels' of volcanic rocks with intervening domes cored by synvolcanic and/or syntectonic plutonic rocks, chiefly gabbro-diorite, tonalite and granite, alternating with east-trending bands of turbiditic wacke (Ayer et al., 2002; Daigneault et al., 2004; Goutier and Melançon, 2007). The volcanic and sedimentary units typically dip sub-vertically, and are separated by abrupt, variably dipping east-trending fault-zones. Some of these fault-zones, such as the Porcupine-Destor and Larder Lake-Cadillac, show evidence of overprinting deformation events including early thrusting, later strike-slip and extension events (Goutier, 1997; Benn and Peschler, 2005; Bateman et al., 2008).
The Abitibi Greenstone Belt/Sub-province is subdivided into northern and southern volcanic zones, which U-Pb zircon ages indicate have similar volcanic episodes and plutonic activity between the two parts of the greenstone belt. The greenstone belt is composed of seven discrete volcanic stratigraphic episodes, which from oldest to youngest are as follows: i). Volcanic Episode 1 which is pre-2750 Ma; ii). Pacaud Assemblage from 2750 to 2735 Ma; iii). Deloro Assemblage from 2734 to 2724 Ma; iv). Stoughton-Roquemaure Assemblage between 2723 and 2720 Ma; v). Kidd-Munro Assemblage between 2719 and 2711 Ma; vi). Tisdale Assemblage from 2710 to 2704 Ma; and vii). Blake River Assemblage between 2704 and 2695 Ma. The Abitibi Greenstone Belt is succeeded by two successor basins, namely: the laterally extensive Porcupine Assemblage with early turbidite-dominated units (Ayer et al., 2002); and the aerially more restricted alluvial-fluvial sequences of the Timiskaming-style basins (Thurston and Chivers, 1990).
The Abitibi Subprovince is bounded to the south by the Larder Lake-Cadillac Fault Zone or Cadillac Tectonic Zone, a major crustal discontinuity that separates the Abitibi and Pontiac sub-provinces (Chown et al., 1992; Mueller et al., 1996; Daigneault et al., 2002, Thurston et al., 2008). To the north it is bounded by the Opatica Sub-province, a complex plutonic-gneiss belt formed between 2800 and 2702 Ma (Sawyer and Benn, 1993; Davis et al., 1995), mainly comprising strongly deformed and locally migmatised, tonalitic gneisses and granitoids (Davis et al., 1995).
The known Noranda Mining District deposits that are associated with the Central Volcanic Complex of the Blake River Group. The Central Volcanic Complex (or 'Noranda Volcanic Complex') represents one of the largest volcanic centres of the Blake River Group, with a diameter of ~35 km. It comprises a 7.5 to 9.0 km thick section of bimodal volcanic strata of mostly tholeiitic to mildly transitional affinity, made up of numerous alternating mafic and felsic units, crosscut by syn-volcanic dykes of dioritic and gabbroic composition (Gélinas et al., 1984; Gibson and Watkinson, 1990; Péloquin et al., 1990; Kerr and Gibson, 1993). It is dominated by coherent basalt, andesite and rhyolite flows, intercalated with <5% volcaniclastic deposits. The mafic volcanic rocks are predominantly pillowed and massive flows, whilst rhyolitic units are typically tabular flows and low-relief domes (Spence and de Rosen-Spence, 1975; Kerr and Gibson, 1993). Volcanism took place over a comparably short time span from ~2700 Ma to 2696 Ma (Mortensen, 1993; Lafrance et al., 2005; David et al.., 2006). This volcanic stratigraphy is intruded by the synvolcanic Flavrian and Powell plutons. The former is composed of sill-like intrusions, characterised by shallow east dips, and generally conformable contacts with the overlying volcanic strata (Wilson, 1941). Geochemical and petrographic data indicate the Powell Pluton, which is located south of the Beauchastel Fault, represents a faulted equivalent to the Flavrian Pluton (Spence and de Rosen-Spence, 1975; Goldie, 1978).
This volcanism in the Rouyn-Noranda District occurred in a below-storm-wave-base, presumably in a deep, marine environment, although local shoaling has been postulated on the southern margin of the exposed sequence (Lichtblau and Dimroth, 1980). These volcanic units within the Central Volcanic Complex strike north to NE, are gently folded about east-trending and east-plunging axes, and dip from 5 to 55°E (Spence and de Rosen- Spence, 1975; Gibson and Watkinson, 1990). The Central Volcanic Complex is interpreted to represent a large shield volcano composed of five volcanic cycles, of which cycles 3 and 4 define a 3 km thick cauldron in-fill sequence that is up to 20 km in diameter (Gibson 1989; Peloquin et al., 1990). These volcanic rocks are interpreted to have been deposited within a volcano-tectonic subsidence structure, which is referred to as the Noranda Cauldron (or Noranda Caldera; Dimroth et al., 1982; Gibson, 1990; Gibson and Watkinson, 1990; Kerr and Gibson, 1993). The known VHMS deposits, including Horne, are either located within the Noranda cauldron, or are situated in close proximity to its margins (Kerr and Gibson 1993). Pearson (2005), Daigneault and Pearson (2006), and Pearson and Daigneault (2006) have
proposed that the Noranda Caldera may be superimposed on two larger and older calderas, the New Senator Caldera, which encompasses the 'Noranda Volcanic Complex', and an older caldera, the Misema Caldera, which encloses the entire Blake River Group.
Whilst all of the five volcanic cycles of the Noranda Cauldron are composed of bimodal mafic-felsic successions, the two pre-cauldron volcanic cycles are tholeiitic, whilst the two syn-cauldron cycles are composed of transitional tholeiitic to calc-alkalic andesite to rhyolite suites (Barrett et al.,1991; Barrie et al.,1993). The basal sections of the Noranda cauldron cycles are intruded by the Flavrian pluton, a subvolcanic intrusion, which as stated above is comagmatic with the overlying stratigraphy (Goldie 1976; Kennedy 1985; Paradis et al.,1988). This pluton is postulated to have been the heat source, and possibly also a metal source for the hydrothermal system responsible for the generation of the VHMS deposits (Kennedy 1985). The early trondhjemite phase of the intrusive complex has a U/Pb zircon age of 2700.8 +2.6/-1.0 Ma, whereas post-cauldron rhyolites are dated at 2697.9 +1.3/-0.7 Ma (Mortensen 1993).
The Central Volcanic Complex has a homoclinal dip of 20 to 60°E, and is cut by numerous synvolcanic and synkinematic faults. Many of the faults interpreted to be synvolcanic exerted a strong control on the distribution of intrusive and volcanic units, as well as hydrothermal activity (Gibson 1989). Most of the rocks of the host sequence have been subjected to lower greenschist facies regional metamorphism, with an amphibolite grade contact metamorphic aureole about the 2690 Ma Lac Dufault pluton. This metamorphic aureole does not extend as far west as the Ansil deposit or as far SE as the Horne mine (Galley et al., 2000).
The known deposits fall within two groups, namely the majority that are associated with a bimodal sequence of rhyolite and andesite flows of the Mine Sequence and occur within the Noranda cauldron, a volcanic subsidence structure that is related to an underlying collapsed magma chamber, the Flavrian Pluton. The second group, which includes the Horne massive sulphide orebodies, lie within a sequence of rhyolitic breccias located just south of the subsidence structure. The two are separated by the ENE-WSW Horne Creek Fault. These two groups of deposit share many characteristics, although they also differ.
The first group, the intra-cauldron deposits are small (<5 Mt), Cu-Zn rich and are interpreted to have been developed as concordant 'mounds' in interflow horizons linked to structurally controlled 'cinduits' and are associated with the bi-modal volcanism. The three large (20 to 50 Mt) Horne deposits were formed in a fault bounded, sediment filled graben on the flank of a rhyolite vent complex as Au-Cu rich and Zn poor deposits with bowl shaped morphologies and are associated with felsic volcanics only.
Economic mineralisation is also found in at least 3 separate volcanic cycles.
Individual deposits and their tonnage and grades include:
Ansil - 1.58 Mt @ 7.2% Cu, 0.9% Zn, 27 g/t Ag, 1.6 g/t Au
Vauze - 0.35 Mt @ 2.94% Cu, 0.94% Zn, 24 g/t Ag, 0.7 g/t Au
Norbec - 3.95 Mt @ 2.77% Cu, 4.50% Zn, 48 g/t Ag, 0.7 g/t Au
East Waite - 1.5 Mt @ 4.13% Cu, 3.26% Zn, 31 g/t Ag, 1.8 g/t Au
Old Waite - 1.12 Mt @ 4.70% Cu, 2.98% Zn, 22 g/t Ag, 1.1 g/t Au
F-Shaft - 0.27 Mt @ 3.40% Cu, 8.60% Zn, 46 g/t Ag, 0.3 g/t Au
Amulet C - 0.57 Mt @ 2.20% Cu, 8.54% Zn, 87 g/t Ag, 0.6 g/t Au
Amulet Lower A - 4.69 Mt @ 5.14% Cu, 5.28% Zn, 44 g/t Ag, 1.4 g/t Au
Amulet Upper A - 0.19 Mt @ 2.37% Cu, 6.12% Zn, 46 g/t Ag, 2.0 g/t Au
Amulet 11 - 0.45 Mt @ 3.65% Cu, 2.38% Zn, 29 g/t Ag, 0.71 g/t Au
Millenbach - 3.56 Mt @ 3.47% Cu, 4.33% Zn, 56 g/t Ag, 1.0 g/t Au
Corbet - 2.78 Mt @ 3.00% Cu, 1.96% Zn, 21 g/t Ag, 1.0 g/t Au
Quemont - 13.8 Mt @ 1.32% Cu, 2.44% Zn, 31 g/t Ag, 5.5 g/t Au
Aldermac - 1.88 Mt @ 4.70% Cu, 7 g/t Ag, 0.3 g/t Au
Deldona - 0.09 Mt @ 0.30% Cu, 5.00% Zn, 26 g/t Ag, 4.1 g/t Au
Delbridge - 0.36 Mt @ 0.55% Cu, 8.6% Zn, 69 g/t Ag, 2.4 g/t Au
Gallen - 2.95 Mt @ 0.07% Cu, 4.77% Zn, 22 g/t Ag, 0.7 g/t Au
Mobrun - 8.64 Mt @ 0.63% Cu, 4.66% Zn, 31 g/t Ag, 1.5 g/t Au
Horne (mined) - 54.3 Mt @ 2.22% Cu, 13 g/t Ag, 6.1 g/t Au
Horne 5 Zone - 150 Mt @ 0.1% Cu, 0.7% Zn, 1.3 g/t Au.
A number of these deposits are descibed in individual records elsewhere in the database, e.g.,
Horne and Horne 5,
Amulet,
Ansil,
Millenbach and
Mobrun Bouchard-Hébert.
HISTORY - The company, Noranda Mines was incorporated in 1922 to exploit the Horne deposit, discovered by Edmond Henry Horne in that year on mineral claims he pegged in 1920. The main discovery hole at Horne was actually in late August 1923. It was the second drill hole, collared in massive sulphide, that intersected 40 m @ 9.94 g/t Au, 32.2 g/t Ag, 5.61% Cu. This intersection led to aggressively exploration and by the end of 1924, a Proved + Indicated Reserve of 0.50 Mt (million tonnes) of ore @ 9.25 g/t Au and 5.66% Cu had been delineated (Roberts, 1956). Extraction of copper began on 17 December 1927. In the succeeding years, prospecting in the Main Noranda district led to discovering several outcropping VHMS deposits, including the Amulet Upper A, Amulet C and Old Waite deposits in 1925 (Monecke et al., 2017). Continued exploration discovered of the Amulet F deposit at a shallow depth of 40 m in 1929. The Amulet Lower A deposit was found at a shallow depth of 200 m in 1937 (Monecke et al., 2017). Amulet operations persisted from 1922-1962 producing copper, zinc, gold and silver. Subsequent discoveries in the main Noranda district were based on mapping and interpreting geological relationships combined with geophysical and geochemical methods (Boldy, 1979; Gibson et al., 2007), including Vauze in 1957, Norbec in 1961, Millenbach in 1966, Corbet in 1974, and Ansil in 1981. The latter was among the deepest discoveries of VHMSs globally, at a depth of 1280 m (Monecke et al., 2017). The Horne mine closed in 1976. Most of the other mines have also since closed or sold to smaller operators.
For detail see the reference(s) listed below.
The most recent source geological information used to prepare this decription was dated: 2000.
This description is a summary from published sources, the chief of which are listed below.
© Copyright Porter GeoConsultancy Pty Ltd. Unauthorised copying, reproduction, storage or dissemination prohibited.
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Selected References:
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Bellefleur G, de Kemp E, Goutier G, Allard M and Adam E, 2014 - Seismic Imaging of the Geologic Framework and Structures Related to Volcanogenic Massive Sulfide Deposits in the Archean Rouyn-Noranda District, Quebec, Canada : in Econ. Geol. v.109 pp. 103-119
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Galley, A.G., Jonasson, I.R. and Watkinson, D.H., 2000 - Magnetite-rich calc-silicate alteration in relation to synvolcanic intrusion at the Ansil volcanogenic massive sulfide deposit, Rouyn-Noranda, Quebec, Canada: in Mineralium Deposita v.35, pp. 619-637.
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Kerr D J, Gibson H L 1993 - A comparison of the Horne volcanogenic massive Sulfide deposit and intracauldron deposits of the mine sequence, Noranda, Quebec: in Econ. Geol. v88 pp 1419-1442
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Paradis S, Taylor B E, Watkinson D H, Jonasson I R 1993 - Oxygen isotope zonation and alteration in the northern Noranda district, Quebec: evidence for hydrothermal fluid flow: in Econ. Geol. v88 pp 1512-1525
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Taylor B E, de Kemp E, Grunsky E, Martin L, Maxwell G, Rigg D, Goutier J, Lauziere K and Dube B, 2014 - Three-Dimensional Visualization of the Archean Horne and Quemont Au-Bearing Volcanogenic Massive Sulfide Hydrothermal Systems, Blake River Group, Quebec : in Econ. Geol. v.109 pp. 183-203
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Porter GeoConsultancy Pty Ltd (PorterGeo) provides access to this database at no charge. It is largely based on scientific papers and reports in the public domain, and was current when the sources consulted were published. While PorterGeo endeavour to ensure the information was accurate at the time of compilation and subsequent updating, PorterGeo, its employees and servants: i). do not warrant, or make any representation regarding the use, or results of the use of the information contained herein as to its correctness, accuracy, currency, or otherwise; and ii). expressly disclaim all liability or responsibility to any person using the information or conclusions contained herein.
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