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Galley, A.G., Hannington, M.D., and Jonasson, I.R., 2007, Volcanogenic massive sulphide deposits, in Goodfellow, W.D., ed., Mineral Deposits of Canada:
A Synthesis of Major Deposit-Types, District Metallogeny, the Evolution of Geological Provinces, and Exploration Methods: Geological Association of
Canada, Mineral Deposits Division, Special Publication No. 5, p. 141-161.
VOLCANOGENIC MASSIVE SULPHIDE DEPOSITS
ALAN G. GALLEY1, MARK D. HANNINGTON2, AND IAN R. JONASSON1
1. Geological Survey of Canada, 601 Booth Street, Ottawa, Ontario K1A 0E8
2. Department of Earth Sciences, University of Ottawa, Marion Hall, 140 Louis Pasteur,Ottawa, Ontario K1N 6N5
Corresponding author’s email: [e-mail]
Abstract
Volcanogenic massive sulphide (VMS) deposits, also known as volcanic-associated, volcanic-hosted, and volcanosedimentary-
hosted massive sulphide deposits, are major sources of Zn, Cu, Pb, Ag, and Au, and significant sources for
Co, Sn, Se, Mn, Cd, In, Bi, Te, Ga, and Ge. They typically occur as lenses of polymetallic massive sulphide that form
at or near the seafloor in submarine volcanic environments, and are classified according to base metal content, gold content,
or host-rock lithology. There are close to 350 known VMS deposits in Canada and over 800 known worldwide.
Historically, they account for 27% of Canada’s Cu production, 49% of its Zn, 20% of its Pb, 40% of its Ag, and 3% of
its Au. They are discovered in submarine volcanic terranes that range in age from 3.4 Ga to actively forming deposits
in modern seafloor environments. The most common feature among all types of VMS deposits is that they are formed
in extensional tectonic settings, including both oceanic seafloor spreading and arc environments. Most ancient VMS
deposits that are still preserved in the geological record formed mainly in oceanic and continental nascent-arc, riftedarc,
and back-arc settings. Primitive bimodal mafic volcanic-dominated oceanic rifted arc and bimodal felsic-dominated
siliciclastic continental back-arc terranes contain some of the world’s most economically important VMS districts.
Most, but not all, significant VMS mining districts are defined by deposit clusters formed within rifts or calderas. Their
clustering is further attributed to a common heat source that triggers large-scale subseafloor fluid convection systems.
These subvolcanic intrusions may also supply metals to the VMS hydrothermal systems through magmatic devolatilization.
As a result of large-scale fluid flow, VMS mining districts are commonly characterized by extensive semi-conformable
zones of hydrothermal alteration that intensifies into zones of discordant alteration in the immediate footwall
and hanging wall of individual deposits. VMS camps can be further characterized by the presence of thin, but areally
extensive, units of ferruginous chemical sediment formed from exhalation of fluids and distribution of hydrothermal
particulates.
Résumé
Les gîtes de sulfures massifs volcanogènes (SMV) sont connus sous diverses appellations parmi lesquelles on peut
mentionner les gîtes de sulfures massifs associés à des roches volcaniques, encaissés dans des roches volcaniques ou
logés dans des assemblages volcano-sédimentaires. Ils constituent des sources considérables de Zn, Cu, Pb, Ag et Au,
ainsi que des sources importantes de Co, Sn, Se, Mn, Cd, In, Bi, Te, Ga et Ge. Ils consistent généralement en lentilles
de sulfures massifs polymétalliques formées dans des milieux volcaniques sous-marins, au sein ou à proximité du fond
océanique, et sont classés d’après leur contenu en métaux communs ou en or ou selon la lithologie des roches encaissantes.
Près de 350 gîtes SMV ont été découverts au Canada et plus de 800, de par le monde. Dans l’histoire de la production
minière du Canada, 27 % du cuivre, 49 % du zinc, 20 % du plomb, 40 % de l’argent et 3 % de l’or ont été
extraits de gisements SMV. On trouve de tels gîtes aussi bien dans des terrains volcaniques sous-marins datant de 3,4
Ga que dans les fonds océaniques actuels où de nouveaux gîtes sont en cours de formation. La caractéristique la plus
commune à tous les gîtes de SMV tient à leur formation dans des milieux tectoniques de distension, parmi lesquels on
peut mentionner les fonds océaniques en expansion et les arcs. La plupart des anciens gîtes SMV conservés dans les
archives géologiques se sont formés dans des milieux océaniques et continentaux d’arc naissant, d’arc de divergence
et d’arrière-arc. Quelques-uns des districts à gisements SMV les plus importants dans le monde sur le plan économique
se trouvent dans des terrains océaniques primitifs d’arc de divergence caractérisés par un volcanisme bimodal à dominante
mafique, de même que dans des terrains continentaux d’arrière arc caractérisés par un volcanisme bimodal à dominante
felsique et la présence de matériaux silicoclastiques. La plupart des principaux districts miniers à gisements SMV
consistent en amas de gisements formés dans des rifts ou des caldeiras. Leur regroupement est attribuable à l’existence
d’une source de chaleur commune qui donne naissance à de vastes réseaux de convection de fluides sous le plancher
océanique. Les intrusions subvolcaniques qui produisent cette chaleur peuvent aussi fournir des métaux aux réseaux
hydrothermaux des gîtes SMV par le biais d’un dégagement magmatique de matières volatiles. En raison de l’écoulement
de fluides sur une grande étendue, les districts miniers à gisements SMV se caractérisent souvent par la présence
de vastes zones semi-concordantes d’altération hydrothermale, qui gagnent en intensité pour devenir des zones d’altération
discordantes, dans l’éponte inférieure et l’éponte supérieure immédiates des gisements. Ces districts se distinguent
aussi par la présence d’unités minces mais étendues de sédiments chimiques ferrugineux qui résultent de l’exhalaison
et de la diffusion de particules hydrothermales.
Definition
Volcanogenic massive sulphide (VMS) deposits are also
known as volcanic-associated, volcanic-hosted, and volcano-
sedimentary-hosted massive sulphide deposits. They
typically occur as lenses of polymetallic massive sulphide
that form at or near the seafloor in submarine volcanic environments.
They form from metal-enriched fluids associated
with seafloor hydrothermal convection. Their immediate
host rocks can be either volcanic or sedimentary. VMS
deposits are major sources of Zn, Cu, Pb, Ag, and Au, and
significant sources for Co, Sn, Se, Mn, Cd, In, Bi, Te, Ga,
and Ge. Some also contain significant amounts of As, Sb,
and Hg. Historically, they account for 27% of Canada’s Cu
production, 49% of its Zn, 20% of its Pb, 40% of its Ag, and
3% of its Au. Because of their polymetallic
content, VMS deposits
continue to be one of the most
desirable deposit types for security
against fluctuating prices of different
metals.
VMS deposits form at, or near,
the seafloor through the focused
discharge of hot, metal-rich
hydrothermal fluids. For this reason,
VMS deposits are classified
under the general heading of
“exhalative” deposits, which
includes sedimentary exhalative
(SEDEX) and sedimentary nickel
deposits (Eckstrand et al., 1995).
Most VMS deposits have two components
(Fig. 1). There is typically
a mound-shaped to tabular,
stratabound body composed principally
of massive (>40%) sulphide,
quartz and subordinate phyllosilicates,
and iron oxide minerals and
altered silicate wall-rock. These
stratabound bodies are typically
underlain by discordant to semiconcordant
stockwork veins and
disseminated sulphides. The stockwork
vein systems, or “pipes”, are
enveloped in distinctive alteration
halos, which may extend into the
hanging-wall strata above the VMS
deposit.
VMS deposits are grouped
according to base metal content,
gold content, and host-rock lithology
(Figs. 2, 3, 4). The base metal
classification used by Franklin et
al. (1981) and refined by Large
(1992) and Franklin et al. (2005) is
perhaps the most common. VMS
deposits are divided into Cu-Zn,
Zn-Cu, and Zn-Pb-Cu groups
according to their contained ratios
of these three metals (Fig. 2). The
Cu-Zn and Zn-Cu categories for
Canadian deposits were further
refined by Morton and Franklin
(1987) into Noranda and Mattabi
types, respectively, by including
the character of their host rocks
(mafic vs. felsic, effusive vs. volcaniclastic)
and characteristic alteration
mineral assemblages (chlorite-
sericite dominated vs. sericitequartz
± carbonate-rich). The Zn-
Pb-Cu category was added by
Large (1992) in order to more fully
represent the VMS deposits of
Australia (Fig. 2). Poulsen and
Hannington (1995) created a sim-
A.G. Galley, M.D. Hannington, and I.R. Jonasson
142
BLACK SMOKER COMPLEX
APPROX. LIMIT OF
DEMAGNETIZED ZONE
100 M
ANHYDRITE CONE
DEBRIS APRON & SULFIDE TALUS
METALLIFEROUS SEDIMENT
ALTERATION PIPE
GRADATIONAL CONTACT
SILICIFIED, PYRITIC STOCKWORK
CHLORITIZED ± HEMATIZED BASALT
SEALED
ZONE
Zn-RICH MARGINAL
FACIES
PYRITE
QUARTZ
WHITE SMOKERS
COLLAPSED AREA
ANHYDRITE
FIGURE 1. Schematic diagram of the modern TAG sulphide deposit on the Mid-Atlantic Ridge. This represents
a classic cross-section of a VMS deposit, with concordant semi-massive to massive sulphide lens underlain
by a discordant stockwork vein system and associated alteration halo, or “pipe”. From Hannington et al.
(1998).
Pb Zn
Cu
Zn-Pb-Cu
Zn-Cu
Pb-Zn
Cu
Cu-Zn
SEDEX deposits VMS deposits
Canadian VMS
Pb
Zn-Pb-Cu
Cu
Zn
Zn-Cu
Pb-Zn
Cu
Cu-Zn
SEDEX deposits VMS deposits
100-1000
1000-10 000
>10 000
1-100
World VMS 103 tonnes per 1% area
(Modified from
Franklin, 1996)
FIGURE 2. Base metal classification scheme of worldwide and Canadian VMS deposits as defined by Franklin
et al. (1981) and modified by Large (1992) to include the Zn-Pb-Cu class. The preponderance of Cu-Zn and
Zn-Cu VMS deposits in Canada is due to the abundance of Precambrian primitive oceanic arc settings.
Worldwide, there is a larger proportion of felsic-hosted, more Pb-rich continental rift and continent margin
arc settings.
Volcanogenic Massive Sulphide Deposits
143
ple bimodal definition of “normal” versus “Au-rich” VMS
deposits (Fig. 3). This originally was intended to identify
deposits that are transitional between VMS and epithermal
deposits (e.g. Sillitoe et al., 1996) (Fig. 4). Further research
has indicated a more complex spectrum of conditions for the
generation of Au-rich VMS related to water depth, oxidation
state, the temperature of the metal-depositing fluids, and
possible magmatic contributions (e.g. Hannington et al.,
1999a). In the classification of Poulsen and Hannington
(1995) Au-rich VMS deposits are arbitrarily defined as those
in which the abundance of Au in ppm is numerically greater
than the combined base metals (Zn+Cu+Pb in wt.%, Fig. 3).
A third classification system that is gaining acceptance is a
five-fold grouping first suggested by Barrie and Hannington
(1999), and later modified by Franklin et al. (2005). This
system classifies VMS deposits by their host lithologies
(Fig. 4), which includes all strata within a host succession
defining a distinctive time-stratigraphic event (Franklin et
al., 2005). These five different groups are bimodal-mafic,
mafic-backarc, pelitic-mafic, bimodal-felsic, and felsic-siliciclastic.
To this is added a sixth group of hybrid bimodal
felsic, which represent a cross between VMS and shallowwater
epithermal mineralization (Fig. 4). These lithologic
groupings generally correlate with different submarine tectonic
settings. There order here reflects a change from the
most primitive VMS environments, represented by ophiolite
settings, through oceanic rifted arc, evolved rifted arcs, continental
back-arc to sedimented back-arc.
Geographical Distribution
There are close to 850 known VMS deposits worldwide
with geological reserves of over 200,000 t. They are located
in submarine volcanic terranes that range in age from the 3.4
Ga Archean Pilbara Block, Australia, to actively forming
deposits in modern seafloor spreading and oceanic arc terranes
(Fig. 5, Table 1). VMS-epithermal hybrids are also
forming today in volcanically active shallow submarine
(Manus Basin) and lacustrine environments. VMS deposits
are recognized on every major continent except Antarctica,
although Zn-Pb-Cu deposits are forming in the Bransfield
Strait adjacent to the Antarctic Peninsula (Peterson et al.,
2004). Cu and Au have been produced from Tertiary-age
deposits hosted in ophiolites around the eastern
Mediterranean and Oman for over 5000 years. Prior to 2002,
VMS deposits are estimated to have supplied over 5 billion
tonnes of sulphide ore (Franklin and Hannington, 2002).
This includes at least 22% of the world’s Zn production, 6%
of the world’s Cu, 9.7% of the world’s Pb, 8.7% of its Ag,
and 2.2% of its Au (Singer, 1995).
Over 350 deposits and major VMS occurrences containing
geological reserves of more than 200,000 tonnes are
known in Canada, of which only 13 are producing mines as
of 2006 (Fig. 6, Table 2). Of these, Louvicourt, Bouchard-
Hébert, Selbaie, and Konuto have been closed. VMS
deposits are known to occur in every province and territory
except Alberta and Prince Edward Island. The largest number
of deposits is in Quebec (33%), followed in descending
order by Manitoba (15%), Newfoundland (12%), British
Columbia (10%), Ontario (9%), and New Brunswick (9%).
The deposits in New Brunswick have had the highest aggregate
metal value (Cu+Zn+Pb), followed by Quebec and then
Ontario (Fig. 7).
Grade and Tonnage
The over 800 VMS deposits worldwide range in size from
200,000 tonnes to supergiant deposits containing more than
150 million tonnes (Franklin et al., 2005) (Table 3). Among
the largest is Rio Tino, Spain’s portion of the Iberian Pyrite
Belt (IPB), with contained ore in excess of 1.535 Bt. The
richest supergiant produced to date is Neves Corvo on the
Portuguese side of the IPB, with ore in excess of 270 Mt,
with 8.8 Mt of contained metal. At the average metal prices
to date for 2006 (Cu=$1.75/lb, Zn=$1.25/lb, Ag=$6.00/oz),
this orebody was originally worth in the order of 26 billion
dollars (US). Other large districts are the Urals and Rudny
Altai of Russia and Kazakhstan with over 70 Mt of contained
metals each (Fig. 5). Canada has two supergiant VMS
deposits (Windy Craggy and Brunswick No. 12) and two
giant VMS deposits (Kidd Creek, and Horne), which are
defined as being in the upper 1% of the world’s VMS
deposits with respect to total original reserves (Fig. 10A). In
Canada, the largest VMS mining district is Bathurst, New
Brunswick, which contained over 320 Mt of geological
resource of massive sulphide containing 30 Mt of combined
Zn, Cu, and Pb (Figs. 6, 10A). The 128 Mt Brunswick No.
12 deposit alone contained 16.4 Mt of metal (Table 2). This
is followed by the 138.7 Mt Kidd Creek deposit containing
12.6 Mt of metal. The largest known Canadian VMS deposit
is the 297 Mt Windy Craggy deposit, but it contains only 4.1
Mt of Cu, Co, and Au. The 50 Mt Horne deposit contains 2.2
Mt of Zn+Cu+Pb, along with over 330 t of Au, making it
also a world-class gold deposit (Fig. 10B). The 98 Mt
LaRonde VMS deposit contains 258 Mt of gold, and because
of its high Au/base metal ratio (Au ppm/Zn+Cu+Pb% = 1.9)
it is classified by its owner as a gold deposit rather than a
VMS deposit.
Determining the mean and median metal concentrations
for Canadian VMS deposits is difficult due to missing or
Cu+Zn+Pb (%)
AURIFEROUS
Silver (ppm)
Gold (ppm)
ESKAY CREEK
RAMBLER CONS
LA RONDE
BOLIDEN
HORNE
FLIN FLON
BOUSQUET NO 2
MT MORGAN
FIGURE 3. Classification of VMS deposits based on their relative base metal
(Cu+Zn+Pb) versus precious metal (Au, Ag) contents. Some of Canada’s
better known auriferous deposits (underlined) are compared to international
examples. Despite having produced 170 t of Au, the Flin Flon deposit is not
considered an auriferous VMS deposit under this classification. Modified
from Hannington et al. (1999c).
incomplete data for a large number of deposits. Pb grades are
known for 34% of Canadian deposits, whereas 55% have
known Au grades and 75% have known Ag grades. From the
available production data, the mean and median (in brackets)
size and grades for past and present producing Canadian
deposits are 7 306 521 t grading 4.88% (4.12) Zn, 1.62%
(0.70) Cu, 1.639% (1.00) Pb, 63 g/t (37) Ag, and 1.65 g/t
(0.88) Au. Figure 9B shows the more meaningful breakdown
of tonnage and grade for each of the five Canadian VMS
types as defined by host lithology. Bimodal mafic deposits
account for the greatest number and, therefore, the largest
aggregate tonnage of the five deposit types, with both siliciclastic
types accounting for the largest average tonnage. The
mafic-siliciclastic deposit types have the highest average
tonnage, with the number highly skewed by Windy Craggy.
As expected, the three deposit types dominated by mafic volcanic
and volcaniclastic rocks have the highest Cu grades,
whereas the two felsic-dominated deposit types contain the
highest Pb and Ag contents. The bimodal felsic deposit
group contains the highest average gold. Mafic-ultramaficdominated
systems can also contain Se, Co, and Ni. The
presence of immature sediments (i.e. black shale) within the
footwall stratigraphy can also influence hydrothermal fluid
composition, as is postulated for he Se-rich Wolverine and
KZK deposits in the Finlayson Lake camp (Bradshaw et al.,
2003). Possible contributions from devolatilizing subvol-
A.G. Galley, M.D. Hannington, and I.R. Jonasson
144
Canadian grade
and tonnage
Canadian grade
and tonnage
500 m
0.98% Cu
4.7% Zn
2.0% Pb
53 g/t Ag
0.93 g/t Au
Hematite
Iron formation facies
Magnetite
Carbonate
Manganese-iron
Carbonaceous shale
Siliceous stockwork
Chlorite-pyrrhotite-pyrite
Massive fine-grained and -chalcopyrte-(Au)
layered pyrite
Layered pyrite-sphaleritegalena-
Ag-Au (transitional ore)
Massive pyrrhotite-pyritechalcopyrite-(
Au)
Felsic volcaniclastic
and epiclastic
Alkaline basalt
Argillite-shale
Felsic epiclastic
Basement sediments
Average 9.2 Mt
Median 64.4 Mt
FELSICSILICICLASTIC
Sericite-quartz
Chalcopyrite-pyrrhotite-pyrite
Pyrite-sphalerite-chalcopyrite
Pyrite-sphalerite-galena
Pyrite-sphalerite-galena
tetrahedrite-Ag-Au
Chlorite-sericite
Quartz-chlorite
Barite (Au)
Carbonate/
gypsum
1.3% Cu
6.1% Zn
1.8% Pb
123 g/t Ag
2.2 g/t Au
Average 5.5 Mt
Median 14.2 Mt
100 m
Felsic flow complex
Flows or volcaniclastic strata BIMODAL-FELSIC
Sericite-quartz-pyrite
(argillic)
Quartz-pyrite-arsenopyritesphalerite-
galena-tetrahedrite veins
Arsenopyrite-stibnitetetrahedrite-
Pb sulphosalts
Quartz-sericie- Realgar-cinnabar-stibnite
Al silicate
(advanced argillic)
HYBRID
BIMODAL-FELSIC
200 m
3.2% Cu
1.9% Zn
0.0% Pb
15 g/t Ag
2.5 g/t Au
Average 1.3 Mt
Median 2.3Mt
Canadian grade
and tonnage
Sphalerite-chalcoppyrite
-rich margin
Pyrite-quartz breccia
Pyrite-quartz in situ breccia
Massive pyrite
Quartz-pyrite stockwork
Chlorite-pyrite stockwork
Banded jasperchert-
sulphide
Chlorite-sericite alteration
+ jasper infilling
Pillowed mafic
flows
100 m
1.7% Cu
5.1% Zn
0.6% Pb
45 g/t Ag
1.4 g/t Au
Sericite-chlorite
Chlorite-sulphide
Quartz-chlorite
Massive magnetitepyrrhotite-
chalcopyrite
Massive pyritepyrrhotite-
chalcopyrite
Massive pyrite-sphalerite
-chalcopyrite
Sulphidic tuffite/exhalite
Pyrrhotite-pyritechalcopyrite
stockwork
Lobe-hyaloclastite
rhyolite
Pillowed mafic
flows 200 m
Average 6.3 Mt
Median 113.9 Mt
BACK-ARC BIMODAL-MAFIC
MAFIC
1.6% Cu
2.6% Zn
0.36% Pb
29 g/t Ag
<0.9 g/t Au
Pyrrhotite-pyrite-magnetite
transition zone
Pyrrhotite-pyrite-chalcopyrite zone
Chert-carbonate-sulphide
Pyrite-sphalerite zone
Pyrrhotite-chalcopyrite-pyrite- Massive pyrite zone
sphalerite stockwork zone
Laminated argillite
and shale
Basalt sill/flow
Average 34.3 Mt
Median 148 Mt
PELITICMAFIC
200 m
Canadian grade
and tonnage
Infilling and
replacement
Laminated argillite
and shale
Chalcopyritepyrite
veins
Canadian grade
and tonnage
Massive
Detrital
Felsic
clastic
Felsic
lava
dome
Shale/argillite
FIGURE 4. Graphic representation of the lithological classifications modified from Barrie and Hannington (1999) by Franklin et al. (2005), with the addition
of the hybrid bimodal felsic as a VMS-epithermal subtype of bimodal-felsic. Average and median sizes for each type for representative Canadian deposits
shown, along with average grade.
Volcanogenic Massive Sulphide Deposits
145
canic intrusions may also account for anomalous Se, Sn, In,
Bi, Te, and possibly Au and Sb contents (Hannington et al.,
1999c; Yang and Scott, 2003; Dubé et al., 2004).
Geological Attributes
Tectonic Environment
The most common feature among all types of VMS
deposits is that they are formed in extensional tectonic settings,
including both oceanic seafloor spreading and arc
environments (Fig. 11). Modern seafloor VMS deposits are
recognized in both oceanic spreading ridge and arc environments
(Herzig and Hannington, 1995), but deposits that are
preserved in the geological record formed mainly in oceanic
and continental nascent-arc, rifted arc, and back-arc settings
(Franklin et al. 1998; Allen et al., 2002) (Fig. 11). This is
because during subduction-driven tectonic activity much of
the ancient ocean-floor is subducted, leaving only a few
ophiolite suites as remnant obducted ocean-floor. Examples
of these include the Ordovician Bay of Islands ophiolite in
Newfoundland and the Late Triassic Cache Creek terrane in
British Columbia (Bédard and Hébert, 1996; Nelson and
Mihalynuk, 2004).
Nascent, or early arc rifting, results from the initial
foundering of older thickened oceanic crust, commonly
N o .* D e p os i t / D is t r i c t , C o u n t r y To n n a g e ( M t ) N o .* D ep o s i t / D is t ri c t , C ou n t ry To n n ag e ( M t )
1 Br o o k s R a n g e, A l as k a 35 23 Sk e l le f t e, S w ed e n 70
2 F in la ys o n L a k e, Y u k o n 20 24 O ut o k u mp u - Py h a s a l mi , F i n l a n d 90
3 Wi n d y C r a g g y, B C & G r e e n 's C r e e k , A l as k a 30 0 25 Be r gs l a g e n - O r i ja r vi , S w ed e n & F i n l a n d 11 0
4 N o r t h e r n C o r di l l e r a, B r it i s h C o l um b i a 10 0 26 P r ei s k a , S o u t h A f r ic a 45
5 My r a F a ll s , B r it i s h C o l um b i a 35 27 T r oo d o s , C y p r us 35
6 S h as t a, C a l i f o r n ia 35 28 Bl a c k S e a , T u r ke y 20 0
7 Je r o m e, A r iz o n a 40 29 Sa u d i A r ab i a 70
8 Ce n t r a l M e x ic o 12 0 30 Se ma i l , O ma n 30
9 T a m b o G r a n d e, P e r u 20 0 31 So u t h e r n U r al s, Ru ss i a / K az a h k st a n 40 0
10 A ma z o n ia n c r a t o n , B r a z il 35 32 Ce n t r a l U r al s , R u s s i a 10 0
1 1 S l a v e P r o v in ce , N o r t hw es t T er r it o r i es , N u n a v u t 30 33 Ru d n y A l ta i , K az a h k s t a n / R u s s i a 40 0
1 2 Ru t ta n , M a n i to b a 85 34 A l ta i S h a n , M on g o l ia 40
1 3 F li n F lo n - Sn ow L a k e, M a n it o b a 15 0 35 No r th Q i l ia n , Ch i na 10 0
1 4 G ec o , Ma ni to u w a d g e, O nt a r io 60 36 Sa n j ia n g , C h i n a 50
15 S t u r ge o n L a k e, O nt a r i o 35 3 7 Ba w d w in - L ao ch a n g , Bu r ma / 40
1 6 L a d y sm i th - Rh i ne l a n de r , W is c o ns i n /M i c hi g a n 80 38 H ok u r ok u , J a p an 80
1 7 Ab i t ib i, On ta r i o - Qu e b e c 60 0 39 Be s s h i , J a p a n 23 0
1 8 Ba t h u r st , N e w B r u ns w i c k 49 5 40 Ph i l l ip i n e s a r c 65
1 9 Du n na g e Z o n e, Ne wf o u n d la n d 75 41 - 42 Pi lb a r a, Y i l ga r n W e s t er n Au s t r al ia 75
2 0 I b e r ia n Py r i te B e lt , S p a i n & P o r t u g a l 15 7 5 43 Ce n t r al Q u e e n s l a n d , A u s t r al ia 80
2 1 Av o c a, I r e la n d 37 44 L ac h la n F o l d B e l t , A u s t r al ia 10 0
2 2 T r o n d hj ei m, N o r wa y 10 0 45 Mt . R e a d , T as m a n i a 20 0
46 Si n o - K o r ea n P l a t fo r m 40
* n u m b e r s r e f e r t o F ig u r e 5 ; t o n n a g e i s a p p r o x im a t e
FIGURE 5. Geographical distribution of ancient VMS deposits, with major districts highlighted with respect to known aggregate geological reserves (see Table
1). Modified from Sinclair et al. (1999) and Franklin et al. (2005).
TABLE 1. Major world volcanogenic massive sulphide deposits and districts.
A.G. Galley, M.D. Hannington, and I.R. Jonasson
146
Fig. 2D, E
Fig. 2F
Phanerozoic cover rocks
Mesozoic orogen
Paleozoic orogen
Proterozoic cover rocks
Middle Proterozoic orogen
Early Proterozoic orogen
Archean craton
U.S.A.
U.S.A.
km
0 1000
262
261
258
260
263
259
230
234
233,235
227
245
247,248
231,
232
257
256
250
236
241
243
244
242
246
251-255
249
240
237-239
223
222
228,229
202
146-148
224-226
196-201
203-210,
212 -216
70, 71
194,195
176
169
170
171-175,
177-193
221
217
218
219
220
211
168
29
28
57
59
58
50
31
60
61
62-65
66
68, 69 67
75
73
72
74
76
141
150
166, 167
155, 156
157
158
159
165
160-164
151-154
149
145
142, 143
81
144
83
77-79
80, 82
84-140
32-49, 51-56
30
1-27
FIGURE 6. Distribution of VMS deposits in Canada by geologic province. Numbers correspond to deposits listed in the national VMS database (Appendix 1).
D e p o si t Lo c at i o n ( 1) M t C u Zn P b A g A u A ge
w t .% w t . % w t . % g / t g / t
B r u ns w i c k N o . 1 2 Ba t h u rs t , Ne w B r us w ic k 22 9 .8 0 .4 6 7 .6 6 3 . 01 91 0 .4 6 O r do v i c i a n
K i d d C r e e k A b i t i b i , O n ta r i o 14 9 .3
( 1 8 1 m i n e d +
a l l r es o u r ce s )
2 .8 9 6 .3 6 0 .2 2 92 0 .0 5 A r c h e a n
L aR o n d e ( i nc l . L aR o n de I I ) A b i t i b i , Q ue be c 88 .1 0 .3 2 1 .7 1 40 .9 5 .0 7 A r c h e a n
S e l b a i e A b i t i b i , Q ue be c 47 .3 0 .9 8 1 .9 8 20 0 .9 A r c h e a n
My r a F a l ls G p ., B u t t le L a ke W r a n ge l l ia , B r i t i sh Co l u m b i a 29 .3 1. 83 6. 25 0. 5 5 49 2. 01 D e vo n i a n
T r o u t L a k e T r a ns - H u ds o n O r o ge n , M a n i t ob a 20 1 .8 3 5 .5 9 17 .4 1 .7 3 P a l e op r o t e r o z i c
L o u v i c o u r t A b i t i b i , Q ue be c 19 .3 3 .1 1 .7 1 28 .7 0 .8 3 A r c h e a n
T r i p l e 7 T r a ns - H u ds o n O r o ge n , M a n i t ob a 14 .5 3 .3 2 5 .7 8 37 .7 2 .7 1 P a l e op r o t e r o z i c
Bo u c h a r d - Hé be r t A b i t i b i , Q ue be c 10 .2 2 .1 1 4 .7 9 15 1 .4 A r c h e a n
Ca l l i n a n T r a ns - H u ds o n O r o ge n , M a n i t ob a 9 .1 6 1 .4 1 3. 59 23 . 5 2 .0 8 P a l e op r o t e r o z i c
D u c k P o n d * Ce n t r a l V o l ca n ic B e l t , 5 .2 3 .2 4 5 .9 7 1. 1 61 .5 0 .8 8 O r do v i c i a n
P e r se ve r e n c e G r o up * A b i t i b i , Q ue b ec 5 .1 1. 2 4 15 . 8 2 29 .4 0 .3 8 A r c he a n
E sk a y C r e e k S t i k i n e , B r i t is h C o l u m b i a 4 0 .3 3 5 .4 2 .2 99 8 26 .4 Ju r a ss i c
Be l l A l l a r d A b i t i b i , Q u e b e c 3 .2 1 . 5 13 .7 7 43 .5 0. 7 6 A r c he a n
Ch is e l N or t h T r a ns - H u d so n O r o g e n, M a n i t ob a 2 .8 0. 1 5 9 .3 6 0 .4 2 2 0. 4 P a l e op r o t e r oz i c
K o n u t o T r a ns - H u ds o n O r o ge n , 1 .2 8 5 .2 7 1 .4 4 10 .6 2 .0 9 P a l e op r o t e r o z oi c
( 1 ) I n c l u d es p r o d uc t i o n a n d e s t i ma te d r es e r ve s w he r e a p p l i c a b l e .
* I n p r e p r o d uc t i o n ( 2 0 0 6 )
TABLE 2. Canadian volanogenic massive sulphide deposits presently in production (2005).
Volcanogenic Massive Sulphide Deposits
147
along transform fault sutures (Bloomer et al., 1995). These
early suprasubduction terranes are most commonly observed
in the ancient rock record at the base of oceanic arc assemblages
in which VMS deposits are spatially associated with
isolated extrusive rhyolite complexes near the top of thick
basalt and basaltic andesite successions. The best Canadian
example of these bimodal mafic-dominated caldera settings
is the Paleoproterozoic host succession to the Anderson,
Stall, and Rod VMS deposits in the Snow Lake camp,
Manitoba (Bailes and Galley, 1999). The komatiite-basaltrhyolite
setting for the Archean Kidd Creek deposit is interpreted
to be an early primitive arc setting possibly linked to
an underlying mantle plume (Wyman et al., 1999), or a rare
example of a non-arc VMS setting associated with partial
lithospheric melting above a mantle plume (cf. Iceland).
In the idealized evolutionary stages of arc terrane formation,
extension of the principal arc assemblage is another
common period of VMS formation (Fig. 11). This results in
the formation of calderas in which bimodal mafic extrusive
successions predominate. This is perhaps the most common
arc environment for VMS formation in oceanic arc settings.
Bimodal mafic-dominated VMS-hosting calderas include
the Archean Noranda and the Paleoproterozoic Flin Flon
mining camps (Gibson and Watkinson, 1990; Syme and
Bailes, 1993). Rifting of continental margin arcs, in contrast,
results in the development of more volcaniclastic-rich
bimodal felsic extensional settings. Examples include the
Sturgeon Lake camp in the Archean Wabigoon terrane of
Ontario (Morton et al., 1990; Whalen et al., 2004) and the
Devonian Buttle Lake VMS camp in the Wrangellia Terrane
of British Columbia (Barrett and Sherlock, 1996a). Outside
Canada, the Paleoproterozoic Skellefte mining district in
Sweden (Allen et al., 1996a) and the Cambrian Mount Read
VMS district in Tasmania (Corbett, 1992) are other examples
of rifted continental margin arc settings. Continued extension
in both oceanic and continental margin arc settings
results in the development of back-arc basins. In oceanic arc
settings, mature back-arc ophiolites also can host VMS
deposits. Canadian examples include the Paleoproterozoic
Birch-Flexar-Coronation camp on the Saskatchewan side of
the Flin Flon mining district (Wyman et al., 1999) and Betts
Cove, Newfoundland (Swinden et al., 1988; Bédard et al.,
1998). Well known examples outside Canada include the
Tethyan ophiolites in Cyprus (Troodos), Oman (Semail), and
Turkey (Ergani) (Galley and Koski, 1999, and references
therein).
0
5
10
15
20
25
30
35
Manitoba
New
Brunswick
Newfoundland-
Labrador
Northwest
Territories
Nova Scotia
Ontario
Quebec
Saskatchewan
Yukon
Nunavut
British
Columbia
Province
Total metals (Mt)
6
7
6 1
115
33
35
46
42
12
31
FIGURE 7. Histogram of the total tonnage of base metals from known VMS
deposits per province; also shown are the number of deposits. The aggregate
tonnage was calculated by total metals represent divided by geological
reserves (proven, possible, and probable; non 43-101 compliant).
0 20 40 60 80 100 120 140
500
200
100
50
20
10
5
2
1.0
0.5
0.2
Size in Million Metric Tonnes
Number of Deposits
Kidd Creek, Brunswick 12
Flin Flon, Caribou, LaRonde, Horne, Geco
Windy Craggy
Average ancient sulfide deposit
Typical modern seafloor sulfide deposit
FIGURE 8. Global (proven, possible, and probable; non 43-101 compliant)
size distribution for VMS deposits, with deposits over 50 Mt considered
“very large” (Table 1), those over 100 Mt considered “giant”, and those
over 150 Mt defined as “supergiant”. Atlantis II Deep, Red Sea, is considered
the largest modern example of a seafloor massive sulphide deposit.
Best known examples of Canadian very large, giant, and supergiant
deposits are shown. Modified from Hannington et al. (1995).
109
0.03
8.73
4.7
34.3
7.5
1.2
24
197
9
73
40
300
200
100
25
20
15
10
5
1.49
2.5
2.0
1.5
1.0
0.5 0.34 0.35 0.36
2
2
1.5
1.5
1
1
1
1
1
1
1.5
1.5
0.5
0.5
80
80
60
60
40
40
20
20
3
2
2
1
1
2
2
3
3
4
4
5
5
0.5
0.5
Cu (wt.%)
Cu (wt.%)
Zn (wt.%)
Zn
(wt.%)
Pb (wt.%)
Pb (wt.%)
Ag (g/t)
Ag (g/t)
Au (g/t)
Au (g/t)
TOTAL TONNAGE
in billion tonnes
TOTAL TONNAGE
in billion tonnes
0.18
23.7
5.2
11.0
2.8 5.1
62
284
113
255
97
300
200
100
NUMBER OF DEPOSITS
NUMBER OF DEPOSITS
25
20
15
10
5
1.44
AVERAGE TONNAGE
in million tonnes
AVERAGE
TONNAGE in million
tonnes
2.5
2.0
1.5
1.0
0.5
1.24 1.34
2.60
BIMODALSILICICLASTIC
e.g. Bathurst No. 12,
New Brunswick
BIMODAL-FELSIC
e.g. Myra Falls,
British Columbia
MAFICSILICICLASTIC
e.g. Windy Craggy,
British Columbia
BIMODAL-MAFIC
e.g. Noranda, Quebec
& Kidd Creek, Ontario
BIMODAL-MAFIC
e.g. Preiska,
South Africa &
San Nicolas, Mexico
MAFIC
(Ophiolite type)
e.g. Tilt Cove,
Newfoundland
MAFIC
(Ophiolite type)
e.g. Troodos, Cyprus
BIMODALSILICICLASTIC
e.g. Rio Tinto,
Spain
BIMODAL-FELSIC
e.g. Mount Lyell,
Tasmania
MAFICSILICICLASTIC
e.g. Besshi, Japan
A
B
FIGURE 9. Statistics for VMS deposits grouped by lithologic class (Barrie
and Hannington, 1999): (A) worldwide deposits; (B) Canadian deposits.
A.G. Galley, M.D. Hannington, and I.R. Jonasson
148
NAME COUNTRY Orogen CU
%
PB
%
ZN
%
AU
(g/t)
AG
(g/t)
Orebody Age
(est. Ma)
SUPERGIANT
Rio Tinto (Stockwork) Spain Hercynian 1200.00 0.15 0.15 7.00 320
Rio Tinto (Massive) Spain Hercynian 335.00 0.39 0.12 0.34 0.36 22.00 320
Kholodnina Russia Baikal-Vitim 300.00 0.04 0.79 5.2 750
Windy Craggy (Cu,Co) Canada N.Cordilleran 297.40 1.38 0.25 0.22 3.83 220
Neves Corvo Group Portugal Hercynian 270.00 1.59 0.15 1.41 9.87 320
Gai East Russia Uralides (Hercynian) 269.00 1.2 0.7 1.10 7.70 395
Aljustrel Group (total) Portugal Hercynian 250.00 1.2 1.2 3.2 1.00 38.00 320
Brunswick #12 Canada Appalachian 229.80 0.46 3.01 7.66 0.46 91.00 465
Gai Russia Uralides (Hercynian) 205.00 1.4 0.06 0.5 1.10 7.90 395
La Zarza Spain Hercynian 164.00 1.2 1.1 2.5 1.80 47.00 320
Ducktown USA Grenvillean? (Oecee) 163.34 1 0.9 0.30 3.00 1000
GIANT
Kidd Creek Canada Abitibi (Kenoran) 147.88 2.31 0.22 6.18 0.01 87.00 2714
Horne - No. 5 Zone Canada Abitibi (Kenoran) 144.00 1 0.9 1.40 2698
Ozernoe Russia Baikal-Vitim 130.00 0.01 1.2 6.2 500
Ridder-Sokol Kazakhstan Altaides (Hercynian) 125.00 0.3 2 4 2.50 10.00 400
Zyryanov Kazakhstan Altaides (Hercynian) 125.00 0.4 2.7 4.5 0.13 20.00 395
Gacun China Yidun, Indosinian (Tethyan) 124.00 0.72 4.62 6.66 0.46 157.00 200
Masa Valverde Spain Hercynian 120.00 0.5 0.6 1.3 0.80 38.00 320
Sibai Russia Uralides (Hercynian) 115.00 1 0.04 1.56 0.60 16.00 392
Tharsis Spain Hercynian 110.00 0.5 0.6 2.7 0.70 22.00 320
Yubileinoe Russia Uralides (Hercynian) 107.00 1.9 0.1 1.2 2.50 16.00 392
Uchaly Russia Uralides (Hercynian) 106.00 1.1 3.8 1.10 15.50 392
Madneuli Georgia Caucasian (Tethyan) 102.60 1.29 1.8 0.73 4.31 70
VERY LARGE
Mount Lyell Australia Tasman 98.57 1.17 0.01 0.04 0.39 7.20 495
Rouez France Caledonian 90.74 0.6 1.5 1.50 21.00 600
Aznalcollar Spain Hercynian 90.00 0.51 0.85 1.8 0.48 37.00 320
LaRonde (incl.LaRonde-II) Canada Abitibi (Kenoran) 88.00 0.3 1.7 5.07 40.90 2710
Skorpion Namibia Gariep 85.00 0.71 8.05 752
Podolsk Russia Uralides (Hercynian) 84.10 2.01 0.13 1.3 1.49 27.60 392
Murgul Turkey Pontides (Tethyan) 83.14 0.76 0.05 0.03 0.05 3.70 175
Ruttan Canada Trans-Hudson 82.80 1.37 0.08 1.63 0.49 13.11 1900
Tambo Grande 3 Peru S.Cordilleran 82.00 1 0.3 1.4 0.80 25.00 104
San Nicolas Mexico C.Cordilleran 79.90 1.34 2.27 0.53 30.00 136
Pyhasalmi Finland Svecokarelian 75.70 0.9 0.06 1.9 0.20 14.00 1921
Sotiel Spain Hercynian 75.20 0.56 1.34 3.16 0.21 24.00 320
Los Frailes Spain Hercynian 70.00 0.34 2.25 3.92 62.00 320
Heath Steele Canada Appalachian 69.90 0.98 0.89 2.69 0.54 47.00 465
Ulaan Mongolia Kazakh-Mongol(Hercyn.) 68.00 1.2 2 0.21 53.00 380
Caribou Canada Appalachian 64.69 0.51 1.6 4.29 1.89 51.00 465
Crandon USA Trans-Hudson 63.50 1 6.5 1870
Flin Flon Canada Trans-Hudson 62.93 2.2 4.1 2.85 43.20 1875
Zincgruvan( +Knalla) Sweden Svecokarelian 60.00 3.2 10.4 69.00 1890
Tishin Kazakhstan Altaides (Hercynian) 60.00 0.5 0.9 5.3 0.90 15.00 395
Geco Canada West.Superior (Kenoran) 58.40 1.86 0.15 3.45 50.06 2720
Tambo Grande 1 Peru S.Cordilleran 56.20 1.6 0.3 1 0.50 26.00 104
Deerni (Cu-Co) China Indosinian (Tethyan) 54.00 1.23 1.57 0.42 4.73 260
Horne-H&G Orebodies Canada Abitibi (Kenoran) 53.70 2.2 6.10 13.00 2700
Mount Morgan Australia Tasman 50.00 0.7 0.05 0.1 4.70 0.60 385
Outokumpu(Cu,Zn,Co) Finland Svecokarelian 50.00 3.3 0.005 1.07 0.07 9.00 1970
Artem'yev Kazakhstan Altaides (Hercynian) 50.00 1.4 1.6 2.2 1.20 143.00 375
Lousal Portugal Hercynian 50.00 0.7 0.8 1.4 0.70 21.00 300
LARGE
Britannia Canada N.Cordilleran 49.31 1.08 0.033 0.26 0.34 4.03 150
Novo-Leninogorsk Kazakhstan Altaides (Hercynian) 48.00 0.16 1.43 4.04 1.54 32.80 395
Preiska South Africa Namaqua 47.00 1.7 3.8 0.00 1300
Anyox-Hidden Creek Canada N.Cordilleran 45.95 1.37 0.17 9.92 195
Hanaoka Mine (total) Japan Japan arcs(Tethyan) 43.50 1.2 1.5 4.7 0.40 68.00 15
Aguas Tenidas Spain Hercynian 41.00 1.3 0.91 3.1 0.50 37.00 320
Hongtoushan China Sino-Korean Platform 40.00 1.75 2.4 0.77 32.40 3000
Maleev Kazakhstan Altaides (Hercynian) 40.00 2.3 1.3 7.5 0.75 75.00 390
Orlovskoye Kazakhstan Altaides (Hercynian) 40.00 2.4 0.5 2.1 0.80 47.00 392
Ashele (#1) China Altayshan (Hercynides) 34.00 2.51 2.98 0.57 104.03 375
Xiaotieshan China Tarim-NorthQilian (Caled.) 34.00 1.26 3.39 5.33 2.28 126.20 440
Arctic (Brooks Range,Ak) USA N.Cordilleran 32.93 4 0.8 5.5 0.70 55.00 365
Rosebery Australia Tasman 32.70 0.58 4.4 14.5 2.70 145.00 495
Liwu China Yidun, Indosinian (Tethyan) 31.00 2.5 0.62 430
Belousov Kazakhstan Altaides (Hercynian) 30.00 2.6 2.4 9.2 2.00 119.00 395
Lokken ( Hoydal) Norway Caledonian 30.00 2.3 0.02 1.8 0.29 19.00 450
Jerome- United Verde USA Yavapai 30.00 4.8 0.2 1.37 49.70 1800
Bald Mountain USA Appalachian 29.98 1.03 <0.05 1.12 0.51 14.40 430
Besshi Japan Japan arcs(Tethyan) 29.95 2.6 0.3 0.70 21.00 210
Selbaie Canada Abitibi (Kenoran) 29.90 1.21 1.91 0.63 37.02 2730
Myra Falls Group Canada N.Cordilleran 29.32 1.83 0.55 6.25 2.00 49.00 365
Garpenberg (+Lappberget) Sweden Svecokarelian 29.00 0.3 3.3 5.3 0.65 98.00 1890
Bisha Eritrea Pan African 28.60 1.52 4.63 1.68 46.80 850
Vihanti Finland Svecokarelian 28.10 0.48 0.36 5.12 0.49 25.00 1910
Falun Sweden Svecokarelian 28.10 3 1.5 4 3.00 20.00 1875
Safyanovka Russia Uralides (Hercynian) 27.50 3.04 1.4 1.32 25.00 392
McIlvenna Bay Canada Trans-Hudson 27.23 0.9 0.1 3.27 0.34 16.43 1900
Mattagami Lake Canada Abitibi (Kenoran) 25.60 0.42 5.1 0.30 21.60 2725
Las Cruces ( primary) Spain Hercynian 25.20 1.25 1.69 3.63 0.38 38.00 320
Granduc Canada N.Cordilleran 25.06 1.79 0.021 0.1 0.17 10.63 190
Korbalikhinsk Russia Altaides (Hercynian) 25.00 1.46 2.01 9.81 375
Greens Creek USA N.Cordilleran 25.00 0.32 5.1 13.9 5.61 706.00 220
Mtonnes Ore
(Geol.)
* Modified from Franklin et al., 2005
TABLE 3. Examples of large-tonnage volcanogenic massive sulphide deposits of the World (Canadian deposits in red).
Volcanogenic Massive Sulphide Deposits
149
Continental back-arc settings contain some of the world’s
most economically important VMS districts. These environments
are dominated by bimodal siliciclastic rocks ± iron
formation and include the Ordovician Bathurst camp of New
Brunswick (van Staal et al., 2003) and Finlayson Lake
(Piercey et al., 2001). Examples outside Canada include the
Archean Golden Grove camp in Western Australia (Sharpe
and Gemmell, 2002), the Paleoproterozoic Bergslagen district
of Sweden (Allen et al., 1996b), the Cambro-Ordovician
Mount Windsor district of Queensland (Doyle and McPhie,
2000), the Devono-Mississippian Iberian Pyrite Belt
(Carvalho et al., 1999), and parts of the Devonian Southern
Urals VMS districts of Russia and Kazakhstan (Herrington
et al., 2002; Franklin et al., 2005).
Other extensional environments may form in post-accretion
and/or successor arc settings. Crustal thickening of an
accreted ocean-floor-arc assemblage can result in modification
of the angle of descent of the subducting slab, cessation
of subduction along a section of plate boundary, or a change
in the direction of approach of the colliding plates (Ziegler,
1992; Hamilton, 1995). This process results in the generation
of strike-slip basins in the older arc assemblages.
Magmatism associated with these successor arc basins may
be associated with mineralized porphyry systems (Richards,
2003), and the basins may be infilled with both subaqueous
and subaerial bimodal volcanic rocks. This can result in the
formation of multiple mineral deposit types, including
epithermal and VMS deposits. A good example of this is the
Lower Jurassic Hazelton Group in British Columbia, which
hosts the Eskay Creek Au-rich VMS deposit (Barrett and
Sherlock, 1996b; Nelson and Mihalynuk, 2004). When these
strike-slip fault systems propagate into a continental margin
setting, such as in the modern day Guaymas Basin, Gulf of
California, the strike-slip basins begin to infill with terrigenous
sediment. They can host mafic siliciclastic-hosted VMS
deposits, such as the Triassic Windy Craggy and Green’s
Creek deposits in British Columbia and Alaska, respectively
(Peter and Scott, 1999). These are known as Besshi-type
deposits from the type locality in the fore-deep accretionary
wedge outboard of the Miocene Japanese islands. Other
mafic siliciclastic-hosted VMS deposits occur along modern
sedimented seafloor spreading systems such as Middle
Valley, on the Juan de Fuca Ridge off the British Columbia
coast (Goodfellow et al., 1999).
0.0
0.1
1.0
10.0
100.0
0.01 0.1 1.0 10 100
100 tonnes
10 tonnes
1tonne
1,000
Tonnage (Mt)
Au (g/tonne)
Eskay
Creek
LaRonde-Penna
Bousquet 2 Horne
Flin Flon
Caribou
0.0
0.1
1.0
10.0
100.0
0.01 0.1 1.0 10
10.0 Mt
4.0 Mt
1.0 Mt
100 1,000
Tonnage (Mt)
Cu+Zn+Pb (%)
Brunswick #12
Flin Flon
Geco
Kidd Creek
Ruttan
Caribou
Windy Craggy
A
B
FIGURE 10. Distribution of Canadian VMS deposits with respect to (A)
aggregate base metal grade versus tonnes and (B) contained Au versus
tonnes; most auriferous Au deposits contain >4 g/t Au (green diamonds).
Those containing over 1000 tonnes of Au (yellow diamonds) include both
auriferous VMS deposits and those with moderate Au grades but large tonnages.
Giant and supergiant VMS deposits are identified by name. From
National VMS database (Appendix 1).
Nascent
Arc
Ocean
Island
Ocean
Spreading
Centre
Rifted
Arc
Back-Arc
Spreading
Centre
Mature Oceanic
Arc
Back-Arc
Continental
Arc
Back-Arc
Extension
Epithermal Au
Arc assemblage
Continental crust
Siliciclastic strata
Fe-formation
Granitoid
Mafic-ultramafic
intrusion
Orogenic Au
Porphyry Cu-Au
(+ skarns)
VMS deposits
Ocean crust
Lithosphere
Asthenosphere
Failed, or Incipient Rift A
C
B
FIGURE 11. There are three principal tectonic environments in which VMS
deposits form, each representing a stage in the formation of the Earth’s
crust. (A) Early Earth evolution was dominated by mantle plume activity,
during which numerous incipient rift events formed basins characterized by
early ocean crust in the form of primitive basalts and/or komatiites, followed
by siliciclastic infill and associated Fe-formation and mafic-ultramafic
sills. In the Phanerozoic, similar types of incipient rifts formed during
transpressional, back-arc rifting (Windy Craggy). (B) The formation of
ocean basins was associated with the development of ocean spreading centers
along which mafic-dominated VMS deposits formed. The development
of subduction zones resulted in oceanic arc formation with associated
extensional domains in which bimodal mafic, bimodal felsic, and maficdominated
VMS deposits formed. (C) The formation of mature arc and
ocean-continent subduction fronts resulted in successor arc and continental
volcanic arc assemblages that host most of the felsic-dominated and
bimodal siliciclastic deposits. Thin black arrows represent direction of
extension and thick, pale arrows represent mantle movement. Modified
from Groves et al., 1998
District-Scale Environments
Most, but not all VMS deposits, occur in clusters that
define major mining camps. Sangster (1980) used the distribution
of VMS deposits within well known mining districts
in Canada to indicate that there was a first-order regional
control on their distribution (Fig. 12). In general, the deposit
clusters are restricted to either linear rifts or calderas. These
features are generated by regional thinning of the basement,
decompression melting of the underlying mantle, and generation
of mafic magmas (Fig. 13). In ocean spreading-ridge
settings, these magmas rise to within a few thousand metres
of the seafloor to form elongate gabbroic sills that parallel
the seafloor-spreading axes (Stinton and Detrick, 1992).
Where pre-existing ocean-floor or arc lithosphere is present,
these mafic magmas, at temperatures of 1000 to 1400°C,
may underplate the crust, producing intermediate to felsic
partial melts and bimodal mafic intrusive/extrusive assemblages.
The associated gabbro-diorite-tonalite-trondhjemite
intrusive complexes may rise to within 2 to 3 km of the
seafloor (Galley, 2003, and references therein). Where extension
is taking place in thicker (20-30 km) crust, such as in a
continental back-arc setting, magmas may form mid-crustal
intrusions. These melts may not intrude into their comagmatic
volcanic assemblages but may remain in the underlying
basement rocks. These different scenarios result in multiple
forms of district-scale alteration and deposit characteristics
for a VMS district.
The presence of either mafic or composite high-level subvolcanic
intrusions within a rift or caldera setting will drive
a subseafloor hydrothermal-fluid convection system (Galley,
1993; Alt, 1995) (Fig. 14). Connate seawater in the porous
crust is first heated, causing it to become buoyant. As this
heated water rises up synvolcanic fault structures, cold seawater
is drawn in above the cooling intrusion. These originally
cold, near neutral pH fluids are progressively heated
during their downward migration, interacting with the surrounding
rocks at progressively higher temperatures. The
isotherms above cooling sill complexes are generally horizontal,
resulting in the formation of a stratified, district-scale
semi-conformable alteration zone controlled in extent by the
strike length of the underlying intrusion (Spooner and Fyfe,
1973; Munha and Kerrich, 1980; Lagerblad and Gorbatchev;
1985; Gibson and Watkinson, 1990; Galley, 1993; Alt, 1995;
Brauhart et al., 1998; Bailes and Galley, 1999) (Fig. 14). The
distribution of the resulting alteration mineral assemblages
mimics that of regional metamorphic facies (Spooner and
Fyfe, 1973; Alt, 1995; Hannington et al., 2003) (Fig. 15).
Hydrothermal fluid reaction zones immediately overlying
the intrusions can be altered to amphibolite-facies assemblages,
including Fe-Ca-rich amphibole, clinozoisite, Caplagioclase,
and magnetite (Figs. 15, 16A,B,C). Above this
are Na-Ca-rich greenschist-facies assemblages characterized
by albite, quartz, chlorite, actinolite, and epidote. Closer to
A.G. Galley, M.D. Hannington, and I.R. Jonasson
150
5 km
Flin Flon (80 Mt) Snow Lake (40 Mt)
Hokuroku District (90 Mt)
Matagami (34 Mt)
Noranda (100 Mt)
FIGURE 12. A same-scale comparison of selected VMS districts. A 5 km
diameter circle around each deposit shows the hypothetical area of influence
of proximal-scale alteration about each deposit, all encircled by a
dashed line defining the proposed extent of a regional-scale alteration system
for each camp based on the presence of known felsic volcanic and synvolcanic
formations/intrusions (thin black lines). The Noranda example
corresponds closely to the observed alteration. Modified from Sangster
(1980).
5 k m
2 k m
20 km
Mantle Partial Mel t
Mantle decompressio n
an dm eltin g ( >1300°C )
 
Partial Meltin g o f C rust
Mantle
Crust
Mafic mel t
Felsic melts
FIGURE 13. VMS environments are characterized by tectonic extension at
various scales (open arrows). Extension resulted in crustal thinning, mantle
depressurization, and the generation of basaltic melts. Depending on crustal
thickness and density, these mafic melts ponded at the base of the crust,
resulting in partial melting and generation of granitoid melts. These anhydrous,
high-temperature melts quickly rose to a subseafloor environment
(<3 km below seafloor), where their heat initiated and sustained convective
hydrothermal cells that formed VMS deposits (black arrows).
Volcanogenic Massive Sulphide Deposits
151
the seafloor are zeolite-clay and related subgreenschist mineral
assemblages characterized by K-Mg-rich smectites,
mixed-layer chlorites, and K-feldspar. In some regional
hydrothermal systems, the low-temperature alteration
assemblages closest to the seafloor are dominated by carbonate
species due to precipitation from shallowly circulating
seawater (Fig. 16D). These chemical and mineralogical
changes in the ancient rock record can be further revealed by
mapping shifts in bulk rock oxygen and hydrogen isotope
compositions of the different zones (Green et al., 1983;
Taylor and South, 1985; Aggarwal and Longstaffe, 1987;
Cathles, 1993; Paradis et al., 1993). These stratified alteration
zones can have a strike length of 5 to 50 km and a
thickness of 1 to 3 km in caldera settings (Fig. 15). The size
and areal morphology of the alteration system is a reflection
of the size and areal morphology of the VMS deposit cluster
(Fig. 12). The distribution of VMS deposits within this cluster
depends on synvolcanic fault distribution relative to the
underlying intrusions (Eastoe et al., 1987; Gibson and
Watkinson, 1990; Brauhart et al., 1998; Galley, 2003). Faults
that acted as conduits for volcanic feeder systems were the
focal point for ascent of high-temperature, acidic metalladen
hydrothermal fluids that formed VMS deposits. These
fault systems may have remained active through several
cycles of volcanic and hydrothermal activity. This may have
resulted in several periods of VMS formation at different
stratigraphic levels within the rift or caldera structure.
Mafic-dominated, bimodal mafic, and bimodal felsic host
rocks are dominated by effusive volcanic successions and
accompanying, large-scale hypabyssal intrusions (Fig. 17).
This high-temperature subseafloor environment supported
high-temperature (>350°C) hydrothermal systems, from
which may have precipitated Cu, Cu-Zn, and Zn-Cu- (Pb)
VMS deposits with variable Au and Ag contents. Areally
extensive, 1 to 5 m thick, Fe-rich “exhalites” (iron formations)
may mark the most prospective VMS horizons (Spry
et al., 2000; Peter, 2003) (Fig. 18A). These exhalite deposits
consist of a combination of fine volcaniclastic material,
chert, and carbonates. They formed during the immature
and/or waning stages of regional hydrothermal activity when
shallowly circulating seawater stripped Fe, Si, and some
base metals at <250°C and precipitated them on the seafloor
through extensive, but diffuse, low-temperature hydrothermal
venting. Formation of exhalites on a basalt-dominated
substrate was commonly accompanied by silicification
and/or chloritization of the underlying 200 to 500 m of strata
(Fig. 18B). Examples of this are observed in the Noranda,
Matagami Lake, and Snow Lake VMS camps
(Kalogeropoulos and Scott, 1989; Liaghat and MacLean,
1992; Bailes and Galley, 1999). In felsic volcaniclastic-dominated
terranes, the generation of Fe-formation exhalites was
accompanied by extensive K-Mg alteration of the felsic substrate,
as recorded in the Bergslagen district of Sweden
(Lagerblad and Gorbatschev, 1985) and in the Iberian Pyrite
Belt (Munha and Kerrich, 1980).
+ K,Mg,SO4 - Si,Ca, Na, Fe, Mn 200°C
300°C
400°C
Shallow Intrusion
DEEP CONVECTION
Deep Intrusion
SHALLOW CONVECTION
Magmatic Component?
Epidosite
Amphibolite
Greenschist
Zeolite
Si, Fe, S
+ Si, Ca
+ Ca, Si, Fe,Cu
Fe,Zn,
Cu,Si
Mn,Si,Ni
Mg metasomatism
Silicification
300°C
400°C
Impermeable
barrier
Reservoir
zone
FORMATION OF HYDROTHERMAL CELLS
- Si,Na,Ca,
Fe,Zn,Cu
+ Si,Fe,Mn
5000 m 2000 m 2000 m
Spilitization
+ Na, Mg
200°C
Recharge zone
A
B
C
+ K,Mg,SO4
FIGURE 14. The development and maturation of a generic subseafloor
hydrothermal system involves three stages. (A) The relatively deep
emplacement of a subvolcanic intrusion below a rift/caldera and the establishment
of a shallow circulating, low-temperature seawater convection
system. This results in shallow subseafloor alteration and associated formation
of hydrothermal exhalative sediments. (B) Higher level intrusion of
subvolcanic magmas and resultant generation of a deep-seated subseafloor
seawater convection system in which net gains and losses of elements are
dictated by subhorizontal isotherms. (C) Development of a mature, largescale
hydrothermal system in which subhorizontal isotherms control the
formation of semiconformable hydrothermal alteration assemblages. The
high-temperature reaction zone next to the cooling intrusion is periodically
breached due to seismic activity or dyke emplacement, allowing focused
upflow of metal-rich fluids to the seafloor and formation of VMS deposits.
From Galley (1993).
5370
5360
5340
Northing (UTM)
610 620 630 660 650
Easting (UTM)
640
5350 Clinozoisite
Absent
Prehnitepumpellyit
e
Prehnitepumpellyit
e
Epidote-
Actinolit e
Sub-greenschis t
Greenschis t
Greenschist
Amphibolite
Chlorite-Clinozoisite-
Actinolite
Prehnite-
Pumpellyite
Epidote-
Actinolit e
FIGURE 15. Comparison of regional greenschist-facies hydrothermal alteration
in the Noranda Volcanic Complex with previously mapped metamorphic
isograds (solid lines from Dimroth et al., 1983; Powell et al., 1993).
The distribution of greenschist-facies hydrothermal alteration (shaded) suggests
that interpreted metamorphic zonation is at least partly a product of
early synvolcanic hydrothermal processes. Note that epidote and chlorite in
the pre-cauldron sequence are distinct from those of the mine sequence volcanic
rocks, even though they are well within the epidote-actinolite subfacies
and have been metamorphosed at the same pressure and temperature.
Modified from Hannington et al. (2003).
Mafic, felsic, and bimodal siliciclastic volcanic assemblages
tend to host volumetrically smaller mafic and/or felsic
sill-dyke complexes, and generally contain Zn-Cu-Co
and Zn-Pb-Cu-Ag VMS deposits, respectively. More Cu-rich
deposits, such as Neves Corvo in the Iberian Pyrite Belt, may
also be present in settings proximal to discrete extrusive
complexes. The district-scale semiconformable hydrothermal
systems consist of low-temperature mineral assemblages,
with Mg-K smectite and K-feldspar alteration overlain
by extensive units of low-temperature Fe-Si-Mn
deposits. Other types of iron formation in VMS districts are
interpreted to be products of plume fallout from high-temperature
hydrothermal venting, or collection of hypersaline
brines within fault-controlled depressions on the seafloor
(Peter, 2003). Iron formation horizons can extend for tens of
kilometres, as in the Bathurst VMS camp in New Brunswick
(Peter and Goodfellow, 1996) (Fig. 18C), the Paleoproterozoic
Bergslagen district (Allen et al., 1996b), the Devono-
Mississippian Iberian Pyrite Belt in Spain and Portugal
(Carvalho et al., 1999), and the Mississippian Finlayson
Lake camp, Yukon (Peter, 2003). Mineralogical variations
within these regionally extensive iron formations, from
oxide through carbonate to sulphide, are indicative of proximity
to more focused, higher temperature hydrothermal
vent complexes and also reflect stratification of the water
column in the basin. The mineralogical variations are
accompanied by changes in element ratios such as Fe, Mn,
B, P, and Zn (exhalative component) versus Al and Ti (detrital
clastic component) (Peter and Goodfellow, 1996).
Deposit-Scale Environments
VMS deposits consist of a massive to semimassive
stratabound sulphide lens, and most are underlain by a sulphide-
silicate stockwork vein system (Figs. 1, 4). Within this
broad framework, there is a spectrum of deposit sizes, morphologies,
and compositions, depending on the nature of the
synvolcanic faulting, footwall and host-rock lithology, water
depth, size and duration of the hydrothermal system, temperature
gradients, and degree of preservation. Individual
massive sulphide lenses can be over 100 m thick, tens of
metres wide, and hundreds of metres in strike length. The
135 Mt Kidd Creek deposit begins at the present erosion surface
and extends for over 2000 m downplunge (original
strike length), with the five composite orebodies over 500 m
wide and individual lenses up to 100 m thick. The
stratabound sulphide mound component of a VMS deposit
may have a number of morphologies and variable internal
structure (e.g. Fig. 1). Observations of modern seafloor
hydrothermal vent complexes in effusive, flow-dominated
terranes indicate that the deposits begin to form as a series of
A.G. Galley, M.D. Hannington, and I.R. Jonasson
152
FIGURE 16. (A) High-temperature hydrothermally altered mafic volcaniclastic turbidite (left) overlain by a strongly silicified mafic debris flow 1200 m below
the Chisel-Lost-Ghost VMS horizon, Snow Lake. This is a regional-scale reaction zone overlain by a high-temperature zone of silica precipitation.
(B) Strongly silicified pillows with pipe vesicles infilled with actinolite, epidote, and magnetite, and interpillow hyaloclastite completely replaced by the same
assemblage. This alteration facies directly overlies the subvolcanic Mooshla intrusion, Bousquet VMS camp, Quebec. (C) Epidosite typical of the root zones
of VMS hydrothermal upflow zones in which high fluid/rock ratios have resulted in leaching of lithophile, chalcophile, and low field strength elements from
the strata. (D) Chloritoid-rich zone below the Mattabi deposit, Sturgeon Lake, where Fe-rich hydrothermal fluids overprinted a previously formed carbonaterich
regional alteration zone.
A
D
B
C
Volcanogenic Massive Sulphide Deposits
153
sulphide-silicate-sulphate chimneys (Fig. 19A). These
become structurally unstable with continued growth and collapse,
and coalesce to form a breccia mound (Fig. 19A,C).
Continued circulation of hydrothermal fluids within this
breccia mound results in sealing from seawater by a silica,
clay, and/or sulphate cap. Progressive deposition of metal
sulphides within the mound results in the formation of a
complexly textured, semimassive to massive sulphide
mound. The flow of hydrothermal fluid through the mound
structure commonly results in remobilization of previously
deposited metals along a chemical and temperature gradient
perpendicular to the seawater interface. This process is
referred to as zone refining (Eldridge et al., 1983) and results
in a chalcopyrite±pyrrhotite-rich core and a sphalerite±
pyrite±galena-rich outer zone (Fig. 20). In extreme cases,
much of the base and precious metals can be remobilized out
of the sulphide mound and carried into the seawater column
by venting hydrothermal fluids and spent fluids (hot seawater).
Massive pyritic cores and thin, base- and preciousmetal-
enriched outer margins are a characteristic of VMS
Beauchastel Fault
HorneCreek Fault
Hunter Creek Fault
5363060 654640
5341800
629780
Cycle I + II Andesite/Rhyolite
Mine Sequence Andesite/Rhyolite (Cycle III)
Cycle IV Andesite/Rhyolite (Cycle IV)
Horne Volcanic Sequence
VMS Deposits/Occurrences
Flavrian
Intrusion
Powell
Intrusion
Lac Dufault
Granodiorite
B
A
0 km 5
N
VMS deposits
Pike Lake layered complex
Granodiorite
Granodiorite, quartz monzonite
Gabbro, diorite
Mafic volcanics
Felsic volcanics
Biedelman Bay subvolcanic
intrusive complex
Subvolcanic Intrusions
N
0 km 5
49°50’
91°00’
N 0 km 10
Upper Silurian
- D evonian
Granite
Sedimentary and
volcanic rocks
Gabbro
Sedimentary and
volcanic rocks
Silurian
Sedimentary rocks
Carboniferous
Upsalquitch gabbro
Late Neoproterozoic- Lower Cambrian
Miramichi Group
Cambrian - Lower Ordovician
Middle Ordovician - Lower Silurian
Gabbro Granite Blueschist nappe
Fournier Group
California Lake Group Sheephouse Brook
Group
T etagouche Group
VMS deposits
Bathurst
47º45 '
47º00'
65º30 '
66º37'30"
I
Lake
McLeod Road Fault
Morgan
Lake
Snow
Threehouse
Synclin
54°52'35"
54°45'00"
Richard
Lake
Pluton Sneath
Pluton
Lake
Synkinematic intrusions
Cu and Zn-rich VMS
deposits/occurrences
Rhyolite
Younging direction
Dacite
Basalt and basaltic andesite
Turbidites
Synvolcanic intrusions
Volcaniclastic
N
0 km 2
99°52'30"
100°15'00"
FIGURE 17. Examples of clusters of VMS deposits defining a mining camp.
These include (A) the Archean Noranda camp, with 14 bimodal mafic-type
deposits underlain by the Flavrian-Powell subvolcanic intrusion (Santaguida et
al., 1998); (B) the Paleoproterozoic Flin Flon mining camp, Manitoba, with 17
VMS deposits hosted within a series of block-bounded terranes representing different
stages of oceanic arc development. For this reason, the district contains a
wide variety of VMS deposit types (Syme and Bailes, 1993; Galley and
Jonasson, 2003); (C) the Paleoproterozoic Snow Lake camp, Manitoba, with two
subvolcanic intrusions (Sneath Lake and Richard Lake) that instigated two separate
hydrothermal events and formed 8 bimodal mafic deposits (modified from
Bailes and Galley, 1999); and (D) the Ordovician Bathurst mining camp with 35
deposits dominated by the bimodal siliciclastic deposit type (modified from van
Staal et al., 2003).
A
B
D
C
deposits that have had a protracted thermal history (e.g.
Hannington et al., 1998; Petersen et al., 2000).
Although many VMS deposits have a clastic component,
this is usually subordinate to the massive sulphide facies. In
many cases, such as the hanging-wall orebody at Buttle
Lake, British Columbia (Barrett and Sherlock, 1996a), Kidd
Creek, Ontario (Hannington et al., 1999b), and Louvicourt,
Quebec, these subordinate clastic facies contain a mixture of
sulphide and host-rock fragments (Fig. 19D). Interbedded
sulphide and silicate-rich layers form from erosion and periodic
collapse of a sulphide mound to form sand- to brecciasized
deposits. Examples where these clastic sulphide components
are a dominant part of the deposit include Eskay
Creek and Tulsequah Chief, British Columbia (Barrett and
Sherlock, 1996a; Sebert and Barrett, 1996), and Buchans,
Newfoundland (Walker and Barbour, 1981). In other cases,
finely bedded ore lenses may result from high-temperature
plume fallout of sulphide particles intermixing with
hydrothermal silica, talc, and Mg-smectites, plus ambient
background pelagic sedimentation (Peter, 2003, and references
therein). Similar finely banded ores can also be a product
of dynamic recrystallization of sulphides during regional
deformation events. VMS deposits readily accommodate
strain during regional deformation because of the ductile
nature of massive sulphide bodies, and can therefore display
much higher degrees of recrystallization and remobilization
than the surrounding volcanic and sedimentary strata.
In some cases, VMS deposits do not form on the seafloor
but develop as a result of shallow subseafloor replacement.
This occurs when hydrothermal fluids infill primary pore
space in either extrusive, autoclastic, volcaniclastic, or epiclastic
successions below an impermeable cap. At the Ansil
deposit in the Archean Noranda VMS camp, a succession of
laminated felsic ash flows/turbidites infilled a small faultbounded
rift on the felsic flow complex. Hydrothermal fluid
seepage up the rift margins resulted in unit-by-unit replacement
of the laminated volcaniclastic layers by pyrite, sphalerite,
and silica (Fig. 21A). This sulphide-impregnated unit
was in turn replaced by massive pyrrhotite-chalcopyrite during
a second stage of subseafloor replacement (Galley et al.,
1996) (Fig. 21B). Some exceptionally large massive sulphide
deposits have formed within volcanic depressions
infilled with autoclastic and heterolithologic debris flow and
talus deposits. These include the Horne No. 5 lens (Kerr and
Gibson, 1993) Kidd Creek (Hannington et al., 1999b), and
several orebodies at Buttle Lake (Barrett and Sherlock,
1996a) (Fig. 21C).
Most Canadian VMS deposits are characterized by discordant
stockwork vein systems that commonly underlie the
massive sulphide lenses, but may also be present in the
immediate stratigraphic hanging-wall strata (Fig. 21D).
These stockwork vein systems occur at the centre of more
extensive, discordant alteration zones. They form by interaction
between rising hydrothermal fluids, circulating seawater,
and subseafloor rocks. The alteration zones and attendant
stockwork vein systems may extend vertically below a
deposit for several hundred metres. Proximal hanging-wall
alteration can manifest itself as a semi-conformable halo up
to tens of metres thick (Brunswick No 12, Bathurst) or may
continue above the deposit for tens to hundreds of metres as
a discordant alteration zone (Ansil, Noranda). In some cases,
the proximal alteration zone and attendant stockwork vein
mineralization connects a series of stacked massive sulphide
lenses (Amulet, Noranda; LaRonde, Bousquet) representing
synchronous and/or sequential phases of ore formation during
successive breaks in volcanic activity.
In plan view, proximal alteration zones may form a halo
up to twice the diameter of the massive sulphide lens (Fig.
22), but with deposits such as Chisel Lake, Snow Lake
A.G. Galley, M.D. Hannington, and I.R. Jonasson
154
FIGURE 18. (A) Mine contact tuff exhalite horizon (between white lines)
that overlies the silicified andesites of the Waite Formation, Noranda,
Quebec. (B) Silicified basaltic andesite of the Upper Amulet Formation.,
Noranda, Quebec, as an example of pervasive silica precipitation that
occurred in mafic flows directly underlying tuffaceous exhalite units in
many Precambrian VMS camps. (C) Banded magnetite-chert Fe-formation
overlying the Austin Brook massive sulphide deposit, Bathurst camp (photo
by J.M. Peter).
A
B
C
Volcanogenic Massive Sulphide Deposits
155
camp, or Eskay Creek, British Columbia, footwall alteration
can be volumetrically extensive and many times the diameter
of the massive sulphide lens (Galley et al., 1993). The
morphology of proximal alteration zones can vary widely,
but generally they tend to widen in proximity to the paleoseafloor
surface, suggesting more intensive interaction
between shallowly circulating, or connate, seawater and an
ascending hydrothermal fluid. The internal mineralogical
zonation of the alteration zones is indicative of these mixing
phenomena. A Fe-chlorite-quartz-sulphide±sericite± talc
mineral assemblage is commonly associated with the core of
stockwork vein mineralization, which becomes increasingly
quartz- and sulphide-rich towards the lower contact of the
massive sulphide lens. In some cases, talc and/or magnetite
occur at the base of the massive sulphide lens and the top of
the alteration pipe, as at several of the Matagami district
VMS deposits, the Ansil deposit in the Noranda camp, and
the Late Triassic Chu Chua deposit in the Slide Mountain
terrane of British Columbia. The core zone is cloaked in a
wider zone of Fe-Mg-chlorite-sericite, including phengite in
the part of this zone that encompasses the immediate hanging
wall to the massive sulphide lens. Outboard from this is
a zone rich in sericite, phengite, Mg-chlorite, ±albite, ±carbonate,
and ±barite. This outer zone may also encompass a
portion of the hanging-wall strata above, and lateral to, the
massive sulphide lens.
In shallow-water environments (i.e. <1,500 m water
depth), boiling may have occurred either in the upflow zone
or in the immediate subseafloor. Depending on the extent of
boiling, this can result in vertically extensive pyritic stock-
FIGURE 19. (A) Example of a zoned sulphide chimney from the Endeavour Ridge vent field (I.R. Jonasson). (B) Typical textures from a massive sulphide
mound, Main vent field, Juan de Fuca Ridge. Mineralogical banding is due to incremental chimney growth, with ovoids representing worm casts. Fragment
cemented by later sulphide growth during mound collapse and subsequent invasion by hydrothermal fluid. (C) Clastic sandy sulphide ore from Cretaceous
Aarja deposit, Semail ophiolite, Oman. This common texture is created by repeated mound collapse resulting from anhydrite dissolution and recementing
with later sulphide (photo by I.R. Jonasson). (D) Pyrite-sphalerite clast as part of a proximal debris flow, Louvicourt, Val d’Or. 15 cm metal grid for scale.
100 metres
Po Cp
Py
Sp
Gn
Ba
Alteration pipe
Massive sulphide mound
Former seafloor
FIGURE 20. Mineral zonation commonly observed within VMS deposits;
this zoning is largely a function of hydrothermal fluid temperature and composition.
Temperature gradient results in the zoning of sulphide minerals
within both the discordant stockwork zone and the conformable sulphide
mound. From Lydon (1984).
A B
C D
work zones, possibly with widespread and intense sericitequartz-
pyrite alteration. The extensive sericite-rich alteration
system that underlies the Eskay Creek auriferous VMS
deposit may be a product of extensive subsurface boiling of
hydrothermal fluids, which resulted in the formation of lowtemperature
(<200°C) Sb-Hg-As-Pb sulphosalt-rich ore
lenses (Sherlock et al., 1999). More advanced argillic alteration
may be produced by acidic magmatic volatiles, and this
alteration can lead to distinctive aluminosilicate-rich mineral
assemblages when metamorphosed to greenschist grade. In
the case of the LaRonde deposit, Quebec, “classic” moundtype
Zn-Cu-Au massive sulphide lenses are associated with
extensive zones of metamorphosed argillic alteration containing
pyrite-chalcopyrite-bornite-gold stockwork systems.
This may be the result of shallow subsurface boiling and separation
of a volatile-rich fluid or focused input of oxidized
magmatic fluids (Dubé et al., 2004).
In less extreme cases, distal, low-temperature hydrothermal
alteration assemblages associated with VMS deposits
may be difficult to distinguish from regional greenschistfacies
metamorphic mineral assemblages. When both proximal
and regional semiconformable alteration zones are
affected by amphibolite-grade regional or contact metamorphism,
the originally strongly hydrated alteration mineral
assemblages change into a coarse-grained quartz-phyllosilicate-
aluminosilicate assemblages that are very distinct from
the surrounding unaltered strata (Fig. 23). It then becomes
possible to use the systematic variations in these coarsegrained
metamorphic mineral assemblages as vectors
towards the core of the proximal alteration system or upsection
towards the paleo-seafloor (Hodges and Manojlovic,
1993).
Genetic/Exploration Models
Exploration models for VMS systems have several common
themes despite the large variety of submarine environments
in which the deposits can form. The generation of a
VMS-hosting volcanic complex is a response to focused heat
flow caused by tectonic extension, mantle depressurization,
and the resultant formation of high-temperature mantle
melts, crustal partial melts, and common bimodal volcanic
succession. The large majority of VMS deposits in Canada
form in either bimodal mafic or bimodal felsic volcanic terranes
dominated by basalt-basaltic andesite and rhyolite-rhyodacite.
Prospective VMS-hosting arc terranes are characterized
by bimodal volcanic successions that have a tholeiitic to
transitional tholeiitic-calc alkaline composition. The felsic
volcanics are characterized by low Zr/Y (<7) and low
(La/Yb)N (<6) ratios, with elevated high field strength element
contents (Zr >200 ppm, Y >30 ppm, and elevated
LREE and HREE) typical of high-temperature, reduced
magmas derived from partially hydrated crust (Barrie et al.,
1993; Barrie, 1995; Lentz, 1998). The lower viscosities of
the high-temperature felsic magmas result in rapid ascent
A.G. Galley, M.D. Hannington, and I.R. Jonasson
156
FIGURE 21. (A) Finely bedded tuff partially replaced by massive pyrrhotite-chalcopyrite at the Ansil deposit, Noranda. 15 cm metal plates for scale.
(B) Cranston tuff unit with lit-par-lit replacement and in-filling by firstly by pyrite-sphalerite, followed by pyrrhotite-chalcopyrite, Ansil deposit, Noranda.
(C) Rhyolite clasts cemented by pyrite-sphalerite rich sulphide groundmass, Louvicourt deposit, Val d’Or. 12 cm red magnet for scale. (D) Well developed
pyrrhotite-chalcopyrite vein stockwork zone with intense chlorite alteration of the rhyolite wallrocks, Ansil deposit, Noranda.
A B
C D
Volcanogenic Massive Sulphide Deposits
157
with minimal heat loss into subseafloor settings where
hydrothermal convection can be initiated. For this reason,
most prospective VMS environments are characterized by
high-level sill-dyke swarms, discrete felsic extrusive centres,
and large (>15 km long and 2000 m thick) subvolcanic composite
intrusions. The absence of substantial subvolcanic
intrusions in some camps may be due to poor preservation as
a result of folding and faulting.
The interaction of large volumes of volcanic strata with
seawater within these high-heat extensional environments
results in the formation of district-scale alteration zones that
extend over the strike length of the VMS-hosting extensional
feature (spreading ridge, rift, or caldera). Stacked alteration
zones can have an aggregate thickness of 2000 to 3000 m,
and may be intruded by resurgent phases of the underlying
subvolcanic intrusion. Subvolcanic intrusions themselves
can display textural features indicating high-level
devolatilization and high-temperature magmatic hydrothermal
alteration (quartz-epidote-magnetite-ferroactinolite-sulphides).
In some cases, this devolatilization may contribute
metals to the overlying convective hydrothermal system
(Large et al., 1996; Lydon, 1996; Galley, 2003, and references
therein). Regional semiconformable alteration systems
resemble regional metamorphic zones (zeolite, greenschist,
amphibolite), with increasing grade towards the heat source.
Most Canadian VMS districts have been affected by regional
metamorphism, which has resulted in recrystallization of the
original alteration minerals to greenschist and/or amphibolite
assemblages. In camps such as Noranda, Bousquet,
Sturgeon Lake, Manitouwadge, Snow Lake, Leaf Rapids,
and the western Stikine (Tulsequah Chief), regional metamorphism
or local contact metamorphism of alteration minerals
has produced distinctive coarse-grained mineral assemblages
characterized by such minerals as phlogopite,
cordierite, anthophyllite, muscovite, staurolite, garnet,
andalusite, and kyanite. The metamorphosed alteration can
be distinguished from essentially isochemical regional metamorphic
mineral assemblages by the losses and gains of various
elements during fluid-rock interactions (Fig. 15).
Submarine volcanic stratigraphy that is prospective for
VMS mineralization commonly contains ferruginous exhalative
horizons as an indication of subseafloor hydrothermal
activity. Precambrian VMS-related exhalites are commonly
composed of finely bedded, sulphide-rich tuffaceous material.
More extensive Algoma-type oxide facies Fe-formations
are also common in VMS-prospective back-arc environments
of all ages. Both types of exhalite may form proximal
to massive sulphide deposits or extend for strike lengths
of several kilometres to tens of kilometres (Spry et al., 2000;
Peter, 2003). Proximity to a hydrothermal source in these
formations is indicated by positive inter-element correlation
between hydrothermal components (Eu, Fe, Mn, Pb, Zn, Cd,
Au, Ca, Sr, Ba, P, and CO2) versus clastic components (Si,
Ti, Al, Mg, K, and Zr), increasing chondrite normalized
EuEu* (hydrothermal input), and decreasing Ce/Ce* (seawater
input) towards the source (Peter and Goodfellow,
1996; Peter, 2003). Vertical and horizontal facies vary from
oxide through silicate to carbonate, which in some cases,
also may reflect proximity to focused hydrothermal activity
(Peter, 2003).
Key Exploration Criteria
The following are the major exploration criteria for
Canadian VMS deposits and key attributes of VMS-hosting
volcanic complexes.
The deposits occur in volcanic belts from Late Archean to
Eocene in which extension is indicated by relatively primitive
(tholeiitic to transitional) bimodal volcanism in nascentarc,
rifted-arc, and back-arc environments. Some obducted
seafloor-spreading centres and rifted continental margins are
also prospective.
VMS formation occurs during periods of major oceanclosing
and terrane accretion. These include the Late
Archean (2.8-2.69 Ga), Paleoproterozoic (1.92-1.87 Ga),
Cambro-Ordovician (500-450 Ma), Devono-Mississippian
(370-340 Ma), and Early Jurassic (200-180 Ma).
In effusive flow-dominated settings in oceanic arc and
continental margin arcs, VMS deposits can be associated
with 15 to 25 km long, mafic to composite synvolcanic intrusions.
These intrusions are Na-rich and depleted in low field
strength elements and have low airborne radiometric
responses but commonly show magnetic halos due to surrounding
zones of high-temperature fluid interaction.
Exploration should be focused up to 3000 m upsection in the
comagmatic volcanic suites in the hanging wall of the intrusions.
Rhyolites with high Zr (>300 ppm), negative chondrite-
normalized Eu anomalies, (La/Yb)N values of less than
7, (Gd/Yb)N values of less than 2, and Y/Zr ratios of less
PRE - DEFORMA TION
Felsic Pyroclastics
(Nepisiguit Falls Fm.)
3- 5 k m 1- 3 k m 3- 5 k m
Zone 3
(Phengite+
chlorite)
Zone 2
Fe-chlorite±
sericite
(sulphide
stringer
zone)
Zone 1
(Quartz+
Fe-chlorite)
Zone 3
(Fe-Mg-chlorite+
sericite)
Zone 4
(Phengite+
Mg-chlorite)
Felsic V olcanics
(Flat Landing Brook Fm.)
Zone 3
SulphideZone
FIGURE 22. A schematic composite section through a VMS alteration system
in the Bathurst mining camp as an example of a VMS proximal alteration
zone metamorphosed to greenschist-grade mineral assemblages. From
Goodfellow et al. (2003).
LEGEND
Alteration Facies
Footwall Dacite Chlorite-Staurolite
Biotite-Garnet Siliceous Stringer
Sericite-Kyanite Amphibolite Stringer
50 m
50 m
Massive sulphide lens Chisel Rhyolite
FIGURE 23. A stylized cross-section through the proximal alteration zone at
the Chisel deposit, Snow Lake mining camp, illustrating the changes in
mineral assemblages that occur when the terrane undergoes lower to middle
amphibolite-grade regional metamorphism. From Galley et al. (1993).
than 7 define high-temperature (>900°C) felsic volcanic
environments favourable for VMS formation. The presence
of synvolcanic dyke swarms and exhalite horizons are
indicative of areas of high paleo-heat flow.
In continental back-arc, bimodal siliciclastic-dominated
settings aeromagnetic surveys can be used to identify aerially
extensive iron formations to target hydrothermally
active paleo-seafloor horizons. Variations in the mineralogy
of the iron formations and varying element ratios can serve
as vectors toward high-temperature hydrothermal centres.
Volumetrically minor sill-dyke complexes also may identify
higher temperature hydrothermal centres.
In upper greenschist-amphibolite metamorphic terranes,
distinctive, coarse-grained mineral suites commonly define
VMS alteration zones. These include chloritoid, garnet, staurolite,
kyanite, andalusite, phlogopite, and gahnite. More
aluminous mineral assemblages commonly occur closer to a
high-temperature alteration pipe. Metamorphic mineral
chemistry, such as Fe/Zn ratio of staurolite, is also a vector
to ore. These largely refractory minerals have a high survival
rate in surficial sediments, and can be used through heavy
mineral separation as further exploration guides in till-covered
areas.
Mineralogy and chemistry can be used to identify largescale
hydrothermal alteration systems in which clusters of
VMS deposits may form. Broad zones of semiconformable
alteration will show increases in Ca-Si (epidotization-silicification),
Ca-Si-Fe (actinolite-clinozoisite-magnetite), Na
(spilitization), or K-Mg (mixed chlorite-sericite±Kfeldspar).
Proximal alteration associated with discordant sulphide-
silicate stockwork vein systems includes chloritequartz-
sulphide- or sericite-quartz-pyrite±aluminosilicaterich
assemblages and is typically strongly depleted in Na and
Ca due to high-temperature feldspar destruction. In addition
to geochemical analysis, X-ray diffraction, PIMA, and oxygen
isotope analysis can assist in vectoring towards higher
temperature, proximal alteration zones and associated VMS
mineralization. Although PIMA has been used most effectively
on alteration systems that contain minerals with a high
reflective index, there has been some success in identifying
greenschist-facies minerals within Precambrian VMS
hydrothermal systems (Thompson et al., 1999)
Knowledge Gaps
Researchers have gathered an impressive amount of
knowledge over the last ten years with respect to how, and
where, VMS deposits form within various geodynamic
regimes. This is due to a combination of studies of modern
seafloor environments and detailed and regional-scale studies
of ancient VMS environments. These studies have
allowed us to place VMS depositional environments within
the context of diverse supra-subduction settings that can be
identified in deformed and metamorphosed terranes through
lithostratigraphic facies evaluation and lithogeochemical
analyses. Prospective settings for subseafloor hydrothermal
systems can now be determined through identification of
synvolcanic intrusions that trigger the systems, geochemical
variations in altered rocks and chemical sedimentary horizons,
and the use of mineralogy, geochemistry, and isotope
geology. The fundamental ingredient for the efficient use of
these tools is an appropriate level of understanding of the
architecture of the volcanic terranes. Mapping at 1:20 thousand
scale and complementary geochronological studies of
the Flin Flon, Snow Lake, Leaf Rapids, and Bathurst mining
camps were key to understanding the evolution of the various
VMS-hosting arc assemblages and at what period of
time in this evolution the deposits formed. Detailed lithostratigraphic
mapping was essential in unraveling deformation
histories and understanding the structural repetitions of
prospective ore horizons. At larger scales, we still need a better
understanding of the longevity of hydrothermal systems
and the character and scale of fluid flow into both volcanic
and sedimentary hanging-wall strata. We also need a better
understanding of how to prospect for VMS environments
through thick drift cover using novel heavy mineral analysis
and selective leach methods. Successful exploration under
cover requires improved understanding of the processes of
secondary and tertiary remobilization of metals and trace
elements from a VMS deposit and its associated alteration
system.
Some Areas of High Mineral Potential in Canada
The recognition of new classes of high-sulphidation and
shallow-water VMS deposits and their genetic association
with differentiated magmatic suites in both calc-alkaline and
alkaline volcanic arcs opens up new terranes and volcanic
environments to exploration that were previously considered
non-prospective for VMS. These environments include arc
fronts and successor magmatic arcs in addition to primitive
rifted-arc and back-arc terranes. Calc-alkaline to alkaline terranes,
such as the Triassic Nicola Group and the Lower
Jurassic Hazelton Group in British Columbia, should be
revisited for atypical VMS deposits. Evolved parts of
Archean greenstone terranes, in particular >2.8 Ga terranes
in which there was involvement of early sialic crust, should
also be considered in this context, e.g. Frotet-Troilus
Domain, Grand Nord, North Caribou, and western Slave
subprovinces.
Incipient rift environments of the Paleoproterozoic Trans-
Hudson Orogen: The presence of large volumes of iron formation
and associated VMS mineralization in the Labrador
Trough is evidence of extensive hydrothermal systems generated
in these 2.1 to 2.0 Ga rift systems on both margins of
the orogen. Why did these not develop large VMS deposits
as in other Fe-formation-rich environments (e.g.
Manitouwadge)?
Intrusions associated with Ni-Cu-PGE mineralization represent
large volumes of magma, commonly emplaced at
shallow crustal levels as part of volcano-plutonic complexes.
If emplaced in a subaqueous environment, these terranes
should be highly prospective for mafic siliciclastic or maficdominated
VMS deposits. These may include the submarine
volcanic stratigraphy above the Fox River and Bird River
sills in Manitoba and possibly the Bad Vermilion
anorthositic complex in southwestern Ontario.
Intra-continental back-arc environments have been recognized
as highly prospective for VMS deposits. Where are the
continental back-arc environments in the Superior, Slave,
and Grenville provinces? Have we explored enough in the
>2.8 or <1.5 Ga terranes?
A.G. Galley, M.D. Hannington, and I.R. Jonasson
158
Volcanogenic Massive Sulphide Deposits
159
Terranes affected by thin-skinned fold-thrust tectonics
present special challenges for exploration but are also highly
prospective for VMS deposits. The potential for new exploration
targets in areas such as the Central Volcanic Belt of
Newfoundland is high, and the lessons learned in the Iberian
Pyrite Belt with respect to exploring in such terranes can be
applied in these and other similar terranes in Canada.
The so-called oceanic terranes of British Columbia, such
as the Triassic Slide Mountain and Cache Creek terrane,
should be re-evaluated for their VMS potential in light of the
possibility that they represent back-arc and not ocean-basin
environments. The presence of boninite and subvolcanic
tonalite-trondhjemite intrusions ± rhyolites in these terranes
would be key indicators of possible arc-back-arc systems.
Boninite, in particular, is an indication of a depleted mantle
source typical of nascent to back-arc regimes (Crawford et
al., 1989; Stern et al., 1995; Kerrich at al., 1998; Piercey et
al., 2001).
Acknowledgements
The authors would like to thank many of our colleagues
whose ideas and discussions helped summarize the characteristics
of this fascinating deposit type. They include Jim
Franklin, Wayne Goodfellow, Steve Piercey, Jan Peter,
Benoit Dubé, and Harold Gibson. Jan Peter, and Steve
Piercey are thanked for their insightful reviews of the manuscript.
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