Upload
geoda-santos
View
226
Download
0
Embed Size (px)
Citation preview
7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
1/34
ORIGINAL PAPER
Tellurium-bearing minerals in zoned sulfide chimneys
from Cu-Zn massive sulfide deposits of the Urals, Russia
V. V. Maslennikov & S. P. Maslennikova & R. R. Large &
L. V. Danyushevsky &R. J. Herrington & C. J. Stanley
Received: 21 June 2011 /Accepted: 18 October 2012 /Published online: 22 November 2012# Springer-Verlag Wien 2012
Abstract Tellurium-bearing minerals are generally rare in
chimney material from mafic and bimodal felsic volcanic
hosted massive sulfide (VMS) deposits, but are abundant in
chimneys of the Urals VMS deposits located within Silurianand Devonian bimodal mafic sequences. High physico-
chemical gradients during chimney growth result in a wide
range of telluride and sulfoarsenide assemblages including a
variety of Cu-Ag-Te-S and Ag-Pb-Bi-Te solid solution se-
ries and tellurium sulfosalts. A change in chimney types
from Fe-Cu to Cu-Zn-Fe to Zn-Cu is accompanied by grad-
ual replacement of abundant Fe-, Co, Bi-, and Pb- tellurides
by Hg, Ag, Au-Ag telluride and galen a-fahlore with
native gold assemblages. Decreasing amounts of pyrite,
both colloform and pseudomorphic after pyrrhotite, iso-
cubanite ISS and chalcopyrite in the chimneys is coupled
with increasing amounts of sphalerite, quatz, barite or
talc contents. This trend represents a transition from low-
to high sulphidation conditions, and it is observed across a
range of the Urals deposits from bimodal mafic- to bimodal
felsic-hosted types: Yaman-Kasy Molodezhnoye
Uzelga Valentorskoye Oktyabrskoye Alexandrin-
skoye Tash-Tau Jusa.
Introduction
Tellurium-bearing mineralization is found associated with
many sulfide deposits, particularly in epithermal vein depos-
its of gold and silver (Afifi et al.1988b; Ciobanu et al.2006;
Cook et al. 2007a, b; Jaireth 1991). In general, tellurium-
bearing minerals are relatively uncommon in volca nic-
hosted massive sulfide (VHMS or VMS) deposits (Afifi et
al.1988b; McPhail1995), with the notable exception of the
Urals, where tellurides and tellurium minerals are recordedat a number of deposits (Shadlun 1942; Herrington et al.
1998; Prokin and Buslaev 1999; Moloshag et al. 2002;
Vikentyev2006; Novoselov et al.2006). Tellurium is scarce
in active seafloor hydrothermal systems, and tellurobismu-
thite is recorded rarely in sulfides from the modern oceans
(Iizasa et al.1992).
In the Urals, tellurides are not present in all VMS deposits
(Prokin and Buslaev 1999; Vikentyev 2006). The causes of
this are poorly understood. A theory that tellurides form in
massive sulfide ores during recrystallization caused by late
(low-temperature) hydrothermal or metamorphic processes
(Vikentyev 2006; Eremin 1983) is in contradiction with
the discovery of rich telluride occurrences in some non-
metamorphosed VMS deposits (Shadlun1942; Maslennikov
1999). In previous work (Herrington et al.1998; Maslennikov
et al.1997,2009; Maslennikova and Maslennikov2007), the
authors documented some tellurium-bearing phases in very
well preserved zoned vent chimney fragments from non-
metamorphosed Yaman-Kasy deposit. These results were
highly unusual, but more recently, numerous sulfide chimneys
from a number of unmetamorphosed VMS deposits of the
Editorial handling: L. Danyushevsky
V. V. Maslennikov (*)
Institute of Mineralogy, Ural Devision of RAS,
and the South Ural State University,
Miass, Chelyabinsk district, Russia
e-mail: [email protected]
S. P. Maslennikova
Institute of Mineralogy, Ural Division of RAS,and the South Ural State University,
Miass, Chelyabinsk district, Russia
R. R. Large : L. V. Danyushevsky
CODES ARC Centre of Excellence in Ore Deposits and School
of Earth Sciences, University of Tasmania,
Hobart, Australia
R. J. Herrington : C. J. Stanley
Department of Mineralogy, Natural History Museum,
Cromwell Road,
London SW7 5BD, UK
Miner Petrol (2013) 107:6799
DOI 10.1007/s00710-012-0230-x
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
2/34
Urals have been discovered and are presented here. Diverse
tellurides are abundant in some chimneys but absent in others.
These conflicting data create numerous questions and require
an explanation. The problem can be resolved by research at
different scales including analysis of relevant genetic features
of host sequences, systematic textural and paragenetic studies
of different types of VMS deposits and chimneys, and their
rare mineral assemblages. Paragenetic models, compositionalanalyses and ranges of tellurium-bearing minerals and the
physicochemical interpretation of chimney diversity in differ-
ent types of VMS deposits are the main subjects of this paper.
Methods and samples studied
A preliminary mineralogical study of the samples was fol-
lowed by scanning electron microscopy (REMMA2M
SEM equipped with energy dispersive Xray detector and
JEOL JXA 733) at the Institute of Mineralogy, Russian
Academy of Sciences. Further mineral analyses wereobtained in several laboratories equipped with CAMEBAX
SX50 and JEOL-JXL-8600 (Natural History Museum,
London), Cameca SX-100 (University of Tasmania, Aus-
tralia) and JEOL JXA 8900RL (Freiberg Mining Academy,
Germany). Analytical conditions were similar in the differ-
ent laboratories. In all electron microprobe analyses, the
standard deviation of results is less than 0.1 %. Major and
minor elements were determined at 1525 kV accelerating
potential , 2035 nA beam current and acquisition time
between 10 and 20 s for Xray peak and background. The
effective probe size was between 1 and 2 m.. The follow-
ing standards were used: SK (ZnS), AgL (Ag), SbL
(Sb2S3), CdL(CdS), TeL (Bi2Te3), TeLb (Ag2Te), SeK
(PbSe), BiL(Bi2Te3), PbL(PbS), CuK (CuFeS2), SK
(Bi2S3), AgL (Ag), SbL (Sb2S3), CdL (CdTe), SeK
(Bi2Se3), BiL(Bi2S3), HgMa (HgS) AsKa (GaAs), Cd La
(CdS), MnKa (Mn), CoKa (FeCoNi), TlMa (TlInS2). De-
tection limits were commonly within the following range
(wt%): S and Fe 0.06. Co 0.05, Ni 0.08, Cu 0.10, Zn
0.14, As 0.12, Ag 0.15, Sb 0.090.2, Te 0.120.29,
Hg 0.22, Au 0.18, Pb 0.190.34, Bi 0.180.26, Se
0.10.13, Sn 0.030.05, Hg 0.10.3, Tl 0.27, Sn 0.03,
Mn 0.04.
Quantitative analysis of chimney sulfides and tellurides
for a wide range of major and trace elements (Fe, Cu, Zn,
Co, Ni, Au, Ag, Bi, Pb, Tl, Cd, As, Te, Se, Mo, Sn, V, Ti,
and Mn) was carried out using LA-ICPMS. The instrumen-
tation includes a New Wave 213 nm solid-state laser micro-
probe coupled to an Agilent 7500cs quadrupole ICPMS
housed at the CODES LA-ICPMS analytical facility, Uni-
versity of Tasmania.
The laser microprobe was equipped with an in-house small
volume (~ 2.5 cm3) ablation cell characterised by
7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
3/34
Yaman-Kasy) are ascribed to either a marginal sea (Zaykov
2006) or an island arc (Herrington et al.2005b). The Tagil
and Magnitogorsk zones include a range of arc, back- and
intra-arc rifts (Herrington et al.2005b; Zaykov2006). In the
Sakmara and Tagil arcs, the VMS deposits are hosted in
Silurian age basalt-rhyolite complexes whilst those in the
Magnitogorsk zone are Devonian. The VMS deposits are
situated in extensional graben or half-graben rift valleysnot only in back-arc basins, but also in intra-arc rifted
basement (Maslennikov 1999). The intra-arc rifts contained
infrequently developed calderas (Seravkin 2010). Most of
VMS deposits are located within several stratigraphic levels
(Fig.2).
Urals VMS deposits have been subdivided as into four
main types: Cyprus, Uralian, Besshi and Baymak (note that
names such as Kuroko-type and Altai-type have also
been used in the lite rature to describe the latter type),
depending on the geological and geodynamic conditions of
formation (Glasby et al.2006; Gusev et al.2000; Herrington
et al. 2002, 2005a; Prokin and Buslaev 1999; Seravkin2010; Zaykov2006). These types can be broadly compared
to the classification of Franklin et al. (2005) where Cyprus0
Mafic, Besshi0Pelitic-mafic, Uralian0Bimodal-mafic, and
Baymak0Bimodal-felsic. The Urals VMS deposits where
chimneys were identified are related to the Uralian or
Baymak types. The Uralian and Baymak type deposits
can be subdivided based on the distance between the ore
bodies and basalt basements (Table 1). The distances are
roughly correlated with general ore mineralogy and Te
contents in ore bodies and in the chimneys studied.
The chimneys in situ were found in the central part of
orebodies interpreted as the relics of hydrothermal sulfideFig. 1 The locations of the Urals VMS deposits with documented
chimney occurrences
Fig. 2 The locations of chimney-bearing Urals VMS deposits in compiled stratigraphic columns
Tellurium-bearing minerals in zoned sulfide chimneys 69
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
4/34
mounds degraded on the seafloor (Fig.3). The central part of
the ore lens consists of compact pyrite-chalcopyrite ores
consequently flanked by sulfide breccias and sulfide
turbidites intercalating with ferruginous cherts or black
shales (Maslennikov 1999, 2006; Herrington et al. 2005b;
Buschmann and Maslennikov 2006; Maslennikov et al.
2009). The clastic ores and in-situ massive sulfides collected
from the apex of the sulfide mounds contain abundant frag-
ments of well-preserved chimneys and occasional sulfidized
fauna (Little et al.1997). The lens-like shape of the ore bodies
and the presence of clastic ore with vent fossils indicate that the
Urals VMS deposits were ancient analogues ofblack smoker
sulfide mounds (Shadlun 1991; Zaykov et al. 1995). The
discovery of black smoker chimney fragments confirmed this
hypothesis (Herrington et al.1998; Maslennikov1991,1999,
2006; Maslennikov et al.2009).
Typical features of the Uralian type VMS deposits are a)
common colloform and biomorphic textures of pyrite, relic
Table 1 Te contents in the bulk ore (Data from open reports of
Ministry of Base Metals, USSR) and chimneys (original data by ICP-
MS and LA-ICP-MS analytical techniques) from different types of the
Urals VMS deposits and chimneys (original data from Zaykov 2006;
Maslennikov1999; Moloshag et al. 2002; Tessalina et al.1998,2008;
Vikentyev et al.2000,2004)
VMS Deposit Types Distance from
basalt basement (m)
Mean Te in
ore (ppm)
Mean Te in
chimneys
(ppm)
General ore mineralogy
Yubileynoye Cyprus to
Uaralian
0 30 40 Pyrite, chalcopyrite, sphalerite, marcasite, pyrrhotite,
arsenopyrite, magnetite, tennantite, hessite, and
electrum
Yaman-Kasy Uralian 0100 325 1349 Pyrite, marcasite, chalcopyrite, sphalerite, bornite,
marcasite, arsenopyrite, pyrrhotite, altaite,
tellurobismuthite, coloradoite, empres, site, galena,
site, hessite, tennantite, barite, hematite and magnetite,
galena, enargite, petzite, sttzite, lllingite, volynskite,
greenockite, digenite, cervelleite, benleonardite,
covellite, goldfieldite, sylvanite, frohbergite,
native tellurium, native gold, magnetite
Molodezhnoye Uralian 30120 82 1030 Pyrite, chalcopyrite, sphalerite, bornite, marcasite,
arsenopyrite, pyrrhotite, altaite, tellurobismuthite,
coloradoite, empressite, hessite, tennantite, barite,
hematite, and magnetite, galena, enargite,
stromeyerite, arsenosulvanite, jalpaite, mackinstryite,stannoidite, mowsonite, native gold
Uzelga-4 Uralian 40150 110 358 Pyrite, chalcopyrite, pyrrhotite, altaite,
tellurobismuthite, sylvanite, petzite, coloradoite,
shttzite, hessite, native tellurium, native gold,
tennantite, tetrahedrite, magnetite, arsenopyrite,
coloradoite, siderite,
Oktyabrskoye Uralian to
Baymak
200 30 166 Pyrite, chalcopyrite, bornite, digenite, sphalerite,
quartz, bornite, barite, hessite, altaite, tennantite,
tetrahedrite, native gold
Valentorskoye Uralian to
Baymak
90300 28 196 Pyrite, chalcopyrite, bornite, hessite, tellurobismuthite,
sttzite, empressite or kochkarite, tennantite,
cervelleite, wittichenite, renierite, native gold
Alexandrinskoye Baymak 310 39 28 Pyrite, chalcopyrite, sphalerite, bornite, barite, galena,
tennantite, , hessite, diagenite, stromeyerite, renierite,germanite, acantite, pyrseite, native gold and electrum
Tash-Tau Baymak 150300 5 25 Pyrite, sphalerite, and chacopyrite, bornite, tennantite,
galena, hessite, cervellite, native gold, and electrum,
enargite, galena, digenite, stromeyerite, jalpaite,
germanite, calcite, barite
Saphyanovskoye Baymak or Altai >300 1 17 Pyrite, chalcopyrite, sphalerite, pyrrhotite, galena,
tennatite, tetrahedrite, glauckodot, tellurobismuthite,
hessite and unresolved Bi-telluride, enargite,
stannite, native gold, Pb-sulfosalts
1
Jusa Baymak to
Kuroko
>300 3 0.1 Pyrite, chalcopyrite, sphalerite, galena, tennantite,
tetrahedrite, arsenopyrite, native gold
70 V.V. Maslennikov et al.
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
5/34
phyrrhotite, pseudomorphs of pyrite and marcasite after initial
euhedral pyrrhotite, b) common occurrence of isocubanite
intermediate solid solutions (ISS) and c) low-sulfidation con-
ditions of formation, indicated by the presence of altaite. In the
Baymak-type VMS deposits, colloform and biomorphic pyrite
occurrences are rare, whereas pyrrhotite and pseudomorphs
after pyrrhotite are absent. In the footwall of the Baymak-type
deposits, volcanics are commonly highly altered to quartz-
sericite and sometimes pyrophyllite assemblages with scat-
tered pyrite, chalcopyrite, sphalerite and galena, which form
economically important ores. Abundant galena and fahlores
suggest moderate- to high-sulfidation condition for Baymak-
type deposit formation.
Preservation of chimney material
In the Magnitogorsk and Sakmara zones, the VMS deposits
have been affected by low grade metamorphism, typically to
prehnite-pumpellite facies only. The good preservation of
primary colloform, sulfidized fauna and chimney textures of
the ores is due to this low degree of metamorphic overprint
(Herrington et al.1998; Little et al.1997; Maslennikov et al.
2009; Shadlun 1991; Zaykov 2006). Further north in the
Urals, the rocks of the Tagil arc are dominated by volcanic
units strongly metamorphosed from greenschist to granulite
facies. The Tagil arc, which contains magnetite-rich ferrugi-
nous sediments, is generally metamorphosed to greenschist
facies. Chimney fragments were not found in the Tagil arc,
Dombarovsk and Orsk areas, where the VMS deposits are
metamorphosed to epidote-amphibolite facies. Two excep-
tions to this are the recovery of sulfide chimneys from the
Valentorskoye and Saphyanovskoye deposits. The latter only
shows zeolite facies metamorphism (Grabezhev et al.2001),
and a similar of metamorphic grade is also assumed for the
Valentorskoye deposit. These deposits are located in tectoni-
cally preserved fragments of less-metamorphosed terrains.
Recovery of chimney material is thus restricted to speci-
mens from less metamorphosed VMS deposits, which are
comparable in textural features to modern black and gray
smokers (Herrington et al.1998). In the core of the sulfide
mounds, chimneys are variably recrystallized to granular
pyrite. The most diverse and well-preserved fragments of
sulfide chimneys are instead found within ore breccias. In
sulfide turbidites, the primary colloform and sooty pyrite
fragments of the chimneys were replaced by diagenetic
chalcopyrite, granular pyrite and cryptocrystalline hema-
tite due to seafloor oxidation (Saphina and Maslennikov 2008)
Fig. 3 The position of sulfide
chimneys in the ore bodies from
the Urals VMS deposits
Tellurium-bearing minerals in zoned sulfide chimneys 71
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
6/34
Results
Mineral zonation of chimneys studied
Previous papers have described three Urals chimney frag-
ments where there was clear evidence for high-temperature
fluid flow through the axial zone, passing to a temperature-
zoned chimney wall (Herrington et al. 1998; Maslennikov1999). These authors recognized the presence of three broad
mineralogical zones developed in response to the interaction
of high-temperature vent fluid with seawater.
Chimneys can be broadly divided into three radial
zones described here from the outer wall, formerly in
contact with seawater, to the inner axial hydrothermal
flow cavity: A - external zone typified by pyrite,
marcasite and/or sphalerite; B - internal zone typified
by the presence of chalcopyrite, and C - lining of the
axial zone normally infilled by sphalerite, quartz or
barite. Each of thes e zones may be subdivided into
several subzones in each sample, depending on thepresence of other minerals.
Our new work based on more than 200 well-preserved
chimney/conduit fragments also shows that we can broadly
classify the chimney into 3 types based on mineralogy
(Figs.4 and 5):
Type 1: chalcopyrite-pyrite to quartz-pyrite-chalcopyrite;
Type 2: chalcopyrite-pyrite (marcasite)-sphalerite to quartz-
sphalerite-pyrite-chalcopyrite barite;
Type 3: chalcopyrite-sphalerite to barite-sphalerite-chalcopyrite;
The types form a general range with an increase of
sphalerite abundance from type 1 to type 3. In each type,
the mineralogical variations lead to a decrease in chalcopy-
rite accompanied by an increase in either quartz + pyrite
(type 1 in Fig. 4ad), or sphalerite + quartz (type 2 in
Figs. 4ehand 5ac), or sphalerite + quartz + barite (type
3 in Fig. 5dh). Each type or subtype of these chimneys
exhibits specific mineralogical zonation, loosely adhering to
the broad A, B, C zones classification indicated above.
Mineralogical and textural proxies of the zonation can be
found in the segments of chimney walls (Figs.6,7,8). Each
type of the chimneys contains different rare mineral assemb-
lages (Table2).
Type 1 chimneys
Numerous fragments of chalcopyrite-pyrite chimneys are
present in the Yubileinoye deposit, but the most com-
plete range from chalcopyrite-pyrite to quartz-pyri te-
chalcopyrite chimneys was found in the Yaman-Kasy
deposit. Other type 1 chimney fragments occur in the
lower part of the Saphyanovskoye ore body, and rarely
at the Molodezhnoye, Uzelga-4 and Valentorskoye
deposits. The largest piece of a chimney recovered
measures some 4 cm in diameter and is 12 cm long.
Another typical fragment was found in the sulfide brec-
cia layer on the southern flank of the massive sulfide
lens, measuring some 3-5 cm in diameter, about 4-8 cm
long, and is very strikingly zoned. In cross-section, all
fragments have a simple 23 fold zonation with the
development of A, B and C zones.
Zone A In the chimneys from the Yaman-Kasy deposit, the
outermost zone is composed of laminated and botryoidal
colloform pyrite and the orientation suggests a centrifugal
growth of the botryoidal pyrite (Figs. 6a and 7ac).
Fig. 4 Type 1 (ad) and Types 23 (eh) chimneys specimens from
Yaman-Kasy deposit. Type 1 chimneys: a chalcopyrite-pyrite, b
chalcopyrite-pyrite-marcasite-sphalerite, c marcasite-chalcopyrite-
pyrite-quartz, d quartz-pyrite-chalcopyrite. Type 2 and 3 chimneys:
e chalcopyrite-pyrite-sphalerite; f chalcopyrite-sphalerite-pyrite-
marcasite, g sphalerite-chalcopyrite-marcasite, h quartz-sphalerite-
barite-pyrite-chalcopyrite. a, b, c chimney structural zones (see text
for details). Scale is 1 cm
72 V.V. Maslennikov et al.
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
7/34
Colloform pyrite grades to a vuggy, fine to medium
grained pyrite towards the central part of zone A (sub-
zone A2). The outer layers in the chimneys from the
Saphyanovskoye deposit are made up of botryoidal,
framboidal and dendritic pyrite partly replaced by chal-
copyrite (Fig. 7df). In subzone A2 (Fig. 7a, c, f), there
are rare disseminated tabular-hexagonal crystals of either
nonstochiometric cryptocrystalline pyrite or fine-grained
marcasite, replacing an initial subhedral pyrrhotite
phase. This texture has been also described in modern
chimneys (Peter and Scott 1988; Marchig and Rsch
1988; Paradis et al. 1988), in ores of the Uralian type
deposits (Maslennikova and Maslennikov 2007), and in the
ancient chimney fragments (Maslennikov et al. 2009). The
pseudomorphs contain relic inclusions of pyrrhotite and dis-
play incomplete cleavages in the pyrite, characteristic of for-
mer pyrrhotite crystals (Zhabin and Samsonova1975). Pyrite
net veining and porous textures are typical of pyrite pseudo-
morphs after pyrrhotite crystals (Zierenberg et al. 1993). Chal-
copyrite abundance increases towards the inner rim of zone A
(subzone A3), where idiomorphic coarse-grained pyrite is the
main phase. Euhedral pyrite can contain inclusions of
pyrrhotite. Sphalerite and marcasite are rare to absent in
subzone A3 of chalcopyrite-pyrite chimneys but are abundant
in quartz-rich varieties. The boundary between zones A and B
is distinctive, marked by the disappearance of the granular
aggregates of pyrite.
Fig. 5 Type 2 (ac) and Type 3 (dh) chimneys from the Uselga (a),
Molodezhnoye (b), Saphyanovskoye (c, d), Valentorskoye (e, f), and
Alexandrinskoye (g, h) VMS deposits. a chalcopyrite-pyrite-
sphalerite-quartz, b chalcopyrite-pyrite-sphalerite, c chalcopyrite-
quartz-pyrite-marcasite, d sphalerite-pyrite-chalcopyrite, e
chalcopyrite-sphalerite-quartz, f quartz-sphalerite-pyrite-chalcopy-rite; g sphalerite-chalcopyrite-barite, h sphalerite-chalcopyrite. a,
b, c chimney structural zones (see text for details)
Fig. 6 The most important microfabrics of the chimneys studied:
Yaman-Kasy (af), Oktyabrskoye (g) and Alexandrinskoye (h) deposits.
Reflected lighta reniform colloform pyrite from the outer wall; b
marcasite pseudomorphs after tabular pyrrhotite crystals in the central
part of the outer wall;c subhedral and euhedral pyrite at the boundary
with the chalcopyrite wall;d drusy chalcopyrite with isocubanite lattice;
e kidney-shaped chalcopyrite segregations within sphalerite frame, and
disseminated lllingite in the transition zone between the wall and the
channel; f marcasite pseudomorphs after tabular pyrrhotite crystals in
the sphalerite cement of the channel; g sphalerite with disseminated
chalcopyrite of the outer wall at the contact with crustified chalcopy-
rite of the wall; h graphic intergrowth of chalcopyrite and sphalerite
in the channel
Tellurium-bearing minerals in zoned sulfide chimneys 73
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
8/34
Zone B The interior of the chimneys is formed by rhythmic
layers of coarse-grainedbladeddrusy chalcopyrite (Fig.7).
In chalcopyrite-pyrite chimneys, the outer part (subzone B1),
close to the boundary with zone A, contains cubic crystals of
pyrite only (Yubileynoye, Yaman-Kasy deposits) and is de-void of accessory minerals (Fig. 4a). Sulphoarsenides or/and
tellurides occur in chalcopyrite-pyrite-quartz transitional
members of the series.
In the Saphyanovskoye deposit, glaucodot occurs in such
chimneys whilst in the Valentorskoye deposit, the chimneys
contain Pb-rich tellurobismuthite. Chalcopyrite-pyrite-quartz
chimneys from the Molodezhnoye deposit contain altaite. In
the Yaman-Kasy deposit, the quartz-chalcopyrite-pyrite
chimneys contain disseminated frohbergite, altaite, Sb-rich
tellurobismuthite, sylvanite, sttzite and coloradoite which is
Fig. 7 Wall zonation of type 1 chimneys from the Urals VMS deposits
Fig. 8 Wall zonation of type 2 chimneys from the Urals VMS depos-
its. For legend see Fig. 7
Table 2 Accessory minerals in the chimneys from the Urals VMS
deposits
Minerals Types of VMS deposits
Uralian Baymak
Yb Y S M U V O A TT
Pyrrhotite Fe9S8 + + +
Co- and Te-rich lllingite
(Fe0.8Co0.2)(As1.5Te0.4S0.1)
+
Cobaltite CoAsS +
Arsenopyrite FeAsS + +
Glaucodot (Fe,Co)AsS +
Frohbergite (Fe, Co)Te2 +
Altaite PbTe + + + +
Tellurobismuthite Bi2Te3 + + +
Sylvanite AgAuTe4 + +
Petzite AuAg3Te2 +
Coloradoite HgTe + +
Sttzite Ag5Te3or-phase Ag1.88Te + +
Hessite Ag2Te + + + + + + + +
EmpressiteAgTe + +
Volynskite AgBiTe2 +
Native tellurium Te + +
TeO + Te or Te.H2O +
Native gold Au0.8Ag0.2 + + + + + + + +
CuAg-sulfotellurides +
(CuAgHg)-sulfosalts + +
Tennantite
Cu10(Zn,Fe)2(As,Sb,Te)4S13
+ + + + + + +
Tetrahedrite
Cu10(Zn,Fe)2(Sb,As,Te)4S13
+ + + +
Goldfieldite Cu10Te4S13 +
Greenockite CdS +
Bornite Cu5FeS4 + + + +
Galena PbS + + + + + +
Copper sulfides CuSCu2S + + +
Magnetite FeOFe2O3 + +
Hematite F2O3 +
Deposits: Yb Yubileynoye, Y Yaman-Kasy, V Valentorskoye, M
Molodezhnoye, U Uzelga, O Oktyabrskoye, SSaphyanovskoye, A
Alexandrinskoye,TTTash-Tau
74 V.V. Maslennikov et al.
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
9/34
partly replaced by As, Cu, Ag-sulfosalts (e.g., (Cu,Ag)3AsS4)
related to the enargite group. In quartz-pyrite-chalcopyrite
end-members, tetrahedrite, tennantite and native gold
are common minerals. In the subzone B2, the coarse-
grained chalcopyrite crystals rarely contain pyrite and
accessory mineral assemblages. These are commonly
found in subhedral chalcopyrite crystals of subzone B3.
Zone CThis axial conduit zone is poorly developed in the
chalcopyrite-pyrite chimneys. The position of the axial con-
duit is marked by subhedral marcasite and pyrite or fram-
boidal pyrite (Fig. 7). The open channels located in the
centre of the chalcopyrite-pyrite-quartz and quartz-pyrite
chalcopyrite chimneys are subsequently infilled with subhe-
dral pyrite, marcasite and quartz. In quartz-rich conduits,
tetrahedrite, tennantite, digenite, and bornite occur in asso-
ciation with relics of chalcopyrite.
Type 2 chimneys
The chimneys range from chalcopyrite-pyrite-sphalerite
chimneys to quartz-sphalerite-pyrite-chalcopyrite barite
varieties and are most abundant in the Uralian type of the
VMS deposits (Yaman-Kasy, Uzelga-4, Molodezhnoye, and
the lower level of Saphyanovskoye). Chimneys 210 cm in
diameter and 515 cm long were recovered. Three zones
and several subzones are present in this chimney type
(Figs.4c, dand8).
Zone A This zone shares features with type 1 chimneys. In
chalcopyrite-pyrite-sphalerite chimneys, the outermost sub-
zone A1 is dominated by laminated and botryoidal collo-
form pyrite with interstitial quartz and marcasite (Fig. 8).
However, in some chimneys from the Baymak type deposits
(e.g., Valentorskoye) aggregates of recrystallized dendritic
pyrite are predominant (Fig.8g, h). The fine-grained pyrite
is often quite porous and may be replaced and overgrown by
coarse marcasite. In the middle part (subzone A2), granular
aggregates of pyrite and marcasite enclose very rare pseu-
domorphs after subhedral pyrrhotite (Figs. 6band 8a, b, c,
e). Tetrahedral crystals of chalcopyrite, iron-free sphalerite
and sparry marcasite successively form an epitaxial incrus-
tation on relics of fine-grained colloform pyrite. The cores
of some sphalerite crystals contain emulsion-like chalcopy-
rite forming chalcopyrite disease described in sphalerite
from modern black smoker chimneys (Herrington et al.
1998; Shadlun 1991). The amount of colloform pyrite and
its pseudomorphs after pyrrhotite decline with the increase
in sphalerite at the outer wall of the chimneys. The outer
wall of the sphalerite-rich end-members of this range con-
tains mainly globular colloform, framboidal or/and dendritic
pyrite disseminated in sphalerite and cryptocrystalline quartz
(Maslennikov et al.2009). Colloform pyrite is partly replaced
by anhedral sphalerite, chalcopyrite or quartz in the innermost
part of the zone. Towards the inner part of the outer wall,
coarse-grained marcasite is replaced by euhedral pyrite
enclosed in a chalcopyrite and/or quartz matrix (Fig. 6c). A
galena-tennantite-tetrahedrite assemblage is common for sub-
zones A2 and A3. In the Molodezhnoye deposit, veinlets of
altaite were found in colloform pyrite of pyrite-chalcopyrite-
sphalerite chimneys.
Zone B This zone can be divided into two or three parts
(Fig. 8). The first part (subzone B1) consists of medium-
grained massive or laminated chalcopyrite. Some of the chal-
copyrite layers intercalate with thin interlayers of sphalerite
and/or quartz. Subhedral pyrite, marcasite and accessory min-
erals are common in this subzone. Subzone B2 is composed of
coarse-grained bladed inclusion-free chalcopyrite. This sub-
zone is usually broader in the chalcopyrite-pyrite-sphalerite
members of this chimney type but is commonly absent in the
quartz-sphalerite-pyrite-chalcopyrite barite end-members.
Subzone B3 comprises spear-shaped crystals of chalcopyritewith inclusions of disseminated pyrite and accessory minerals.
In the B1 and B3 subzones, relicts of tartan isocubanite struc-
tures are occasionally observed (Fig. 6d), as was previously
described at Yaman-Kasy (Herrington et al. 1998; Shadlun
1991). Some chimneys from the Molodeznoye, Yaman-Kasy
and Saphyanovskoye deposits contain inclusions of pyrite
pseudomorphs over euhedral pyrrhotite crystals.
In chalcopyrite-pyrite-sphalerite chimneys from the
Yaman-Kasy deposit, subzones B1 and B3 contain telluro-
bismuthite, occasional altaite, frohbergite and sylvanite.
Abundant and diverse rare mineral assemblages are com-
mon in sphalerite-chalcopyrite-pyrite varieties of the
chimneys. Also present are successive overgrowths of co-
baltite, altaite, sylvanite, sttzite, volynskite, native telluri-
um, unresolved black-brown oxide-rich tellurium phases,
and galena. Petzite, empressite, coloradoite and tellurian
lllingite are present occasionally. Tellurobismuthite and
frohbergite are rare, confined to the boundaries with sub-
zone B2. In some chimneys, Ag-sulphotellurides or fine-
grained unresolved Ag-Te-S micrographic phases are found.
A later assemblage comprises native tellurium and gold,
covellite, galena and a newly identified Cu, Pb, Ag, Fe
arsenic-tellurium sulphosalt phase with an approximate for-
mula (Cu, Pb, Hg, Ag,Fe)3 (As,Te)S4. Galena and other
sulphosalts occur together in the outermost part of subzone
B1 and the innermost part of subzone B3. These sulphosalts
replace sulphoarsenides, tellurides, and galena. Mineral di-
versity declines in the barite-rich end member of type 2
chimneys. These quartz-sphalerite-pyrite-chalcopyrite
barite end-members of the chimney range contain mostly
very small grains of hessite, native gold, galena, volynskite,
and tennantite, which are confined to the boundaries be-
tween chalcopyrite and sphalerite. Altaite, arsenopyrite, and
Tellurium-bearing minerals in zoned sulfide chimneys 75
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
10/34
native gold were found in association with hessite, galena
and tennantite in zone B of chalcopyrite-sphalerite-pyrite type
chimneys from the Molodezhnoye deposit. Chalcopyrite-
pyrite-sphalerite-quartz barite chimneys from the Uzelga-4
deposit contain disseminated coloradoite, and very small
grains of tellurobismuthite and gold-rich silver telluride
(probably hessite). In the Saphyanovskoye deposit, small
grains of tellurobismuthite and hessite in association withglaucodot and arsenopyrite have been found. Sulphoarsenides
are replaced by tennantite and tetrahedrite. Tellurides and
arsenides have been replaced by a native gold galena -
tennantite association in sphalerite-pyrite-chalcopyrite
chimneys, found at the upper level of the Saphyanovskoye
deposit. At the boundary with zone C, lllingite occurs in
chalcopyrite, sphalerite and quartz (Fig.6e).
Zon e C The conduits of chalcopyrite-pyrite-sphalerite
chimneys are successively in-filled by pyrite, marcasite, sphal-
erite and occasional quartz (Fig. 8). Quartz-sphalerite-pyrite-
chalcopyrite barite chimneys are characterized by anincreased amount of galena, quartz and euhedral barite.
Sphalerite shows extensive chalcopyrite diseaseand also a
texture consistent with being a pseudomorph after wurtzite
(Herrington et al.1998). Pseudomorphs of marcasite or pyrite
after pyrrhotite are also present in this zone (Fig. 6f). In the
chimneys from the Yaman-Kasy deposit, goldfieldite occurs
in association with a quartz-marcasite assemblage. In the
chimneys of all other deposits, sphalerite-galena-tennantite
assemblages are more common.
In chalcopyrite-pyrite-sphalerite chimneys, the Co- and
Fe-sulfoarsenides and Fe, Co, Bi, Pb-tellurides are replaced
successively by native gold and hessite, and then galena-
sulfosalts assemblages with generally increasing contents of
sphalerite, quartz and barite. The quartz-sphalerite-pyrite-
chalcopyrite barite end-members of this chimney type
resemble the type 3 chimneys.
Type 3 chimneys
This chimney type ranges from chalcopyrite-sphalerite to
quartz-sphalerite -chalcopyrite barite varieties. The main
differences from the previous types are the absence of
marcasite and pyrite pseudomorphs after pyrrhotite. Pyrite
occurs as minor inclusions of euhedral, subhedral pyrite.
Colloform varieties of pyrite are very rare.
Fragments of type 3 chimneys have been collected from
the Alexandrinskoye, Tash-Tau, Jusa , Oktyabrskoye, Val-
entorskoye and Talganskoye deposits. The chimneys are
commonly 2-4 cm in diameter and up to 8 cm in length,
with the largest fragment measuring 10 cm in diameter and
16 cm in length. Mineralogical zones defined from the
exterior to the interior in this type of chimneys are described
below and shown on Fig.9
Zone A The outer wall of this zone comprises predominantsphalerite with disseminated euhedral and subhedral pyrite
(Fig.6g). Barite, quartz, galena and tennantite inclusions are
common for this zone. Rare colloform or framboidal pyrite
occurs only in the outermost subzone of the chimneys. Most
of the original colloform pyrite is replaced by chalcopyrite,
tennantite and galena.
Zone B This chalcopyrite-rich zone is formed by drusy
aggregates of chalcopyrite crystals, successively overgrown
by sphalerite (Fig.6h). The chalcopyrite layers are intercalat-
ed with sphalerite. In chalcopyrite-sphalerite chimneys from
the Valentorskoye deposit, the chalcopyrite contains small
disseminated grains of Pb-rich tellurobismuthite, rare empres-
site and sttzite. In the central parts of this type, hessite and
native gold intergrowth occurs in association with chalcopy-
rite, pyrite, sphalerite and galena. In sphalerite-rich varieties
of these chimneys, galena and Te-rich tennantite are common
mineral inclusions. In the chimneys from the Oktyabrskoye
deposit, chalcopyrite contains rare inclusions of altaite, gale-
na and euhedral pyrite. Chalcopyrite from other deposits is
devoid of accessory minerals. Some chimneys from the Alex-
andrinskoye deposit contain bornite inclusions in association
with euhedral pyrite.
Zone C The conduit zone consists of sphalerite, quartz and
barite. In the Oktyabrskoye deposit, sphalerite contains tellur-
obithmuthite, altaite, galena, and hessite inclusions in associ-
ation with native gold. Galena-tennantite intergrowths in
association with native gold occur in sphalerite of the
chimneys, veinlets and conduits from both Alexandrinskoye
and Tash-Tau deposits (Maslennikova and Maslennikov 2007;
Zaykov 2006). Rare hessite in association with native gold has
been found in sphalerite chimneys from the Alexandrinskoye
Fig. 9 Wall zonation of type 3 chimneys from the Urals VMS depos-
its. Chimneys (d) to (f) are intermediate between Types 2 and 3. For
legend see Fig.7
76 V.V. Maslennikov et al.
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
11/34
deposit. Sphalerite-barite-chalcopyrite chimneys from the
Jusa deposit contain galena and tennantite only.
Composition of tellurium-bearing phases
Te-bearing sufides
We have used SEM and LA-ICP-MS techniques to investigate
the distribution of Te in the chimneys. The most detailed data
were collected by high-resolution LA-ICP-MS analyses of the
Yaman-Kasy deposit (Maslennikov et al.2009). In this paper
we present average contents of Te in chalcopyrite, sphalerite
and pyrite in each main zone of the chimneys from other Urals
VHMS deposits (Table 3). A small number of bornite and
galena grains have also been analyzed by LA-ICP-MS.
Chalcopyrite (CuFeS2) Chalcopyrite is an important host
mineral for Te. The concentrations of Te in chalcopyrite of
the chimneys vary over several orders of magnitude be-tween deposits: Yubileynoye (2560 ppm) Yaman-Kasy
(303200) Uzelga-4 (10250 ) Molodezhnoye (10
2050) Valentorskoye (5550) Octyabrskoye (440)
Alexandrinskoye (
7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
12/34
Table3
MeanTecontentsinsulfid
esfromeachzoneofeachchimneytype(ppm)
Deposit
Chimneytyp
e
Azone
Bzone
Czone
Py
Chp
Sph
Py
Chp
Sph
Py
Ch
p
Sph
Yubileynoye
2
59.1
(16)
0.4
(1)
3.2
(7)
24.3
(6)
3.5
(10
)
23.4
(5)
7.7
(7)
8.7
(2)
4.0
(2)
1
29.7
(12)
2.0
(5)
52.8
(2)
34.3
(10
)
6.8
(2)
186.2
(10)
63.2
(6)
10.0
(5)
1
37.5
(10)
5.9
(3)
57.0
(6)
5.0
(7)
22.0
(1)
Oktyabrskoye
3
281.7
(7)
40.0
(2)
232.4
(5)
693.3
(1)
3.9
(7)
364.7
(2)
103.0
(1)
3.6
(2)
92.7
(4)
TashTau
3
119.0
(9)
0.9
(5)
66.8
(2)
0.1
(12
)
0.0
4(1)
22.4
(3)
0.1
(1)
3
42.4
(5)
0.7
(3)
38.4
(6)
1.5
(9)
3.2
(11)
90.9
(2)
0.4
(3)
6.6
(6)
Valentorskoye
23
160.1
(6)
33.4
(3)
223.5
(2)
1541.6
(5)
41.2
(13
)
296.0
(5)
166.6
(5)
3
67.1
(5)
23
150.0
(9)
5.3
(4)
18.2
(4)
25.7
(14
)
15.7
(5)
127.2
(5)
6.7
(3)
23
440.0
(7)
34.2
(2)
46.0
(2)
405.5
(6)
18.4
(10
)
148.8
(9)
11.6
(1)
22.3
(4)
2
555.7
(8)
541.2
(6)
78.4
(3)
138.7
(8)
52.4
(8)
2
40.2
(2)
38.6
(6)
Molodezhnoye
2
17.9
(7)
1047.9
(8)
616.5
(4)
10734(5)
20
61.9
(1)
412.4
(5)
2
620.2
(14)
17.2
(1)
16.5
(4)
1007.4
(1)
344.7
(12
)
11.2
(1)
360.4
(4)
2
1651.0
(4)
799.5
(3)
218.6
(5)
960.0
(8)
802.5
(3)
7.1
(2)
154.3
(11)
Saphyanovskoye
3
34.3
(7)
2.8
(5)
7.9
(1)
1.0
(3)
0.1
(1)
54.1
(1)
1.3
(3)
4.5
(5)
2
5.9
(14)
0.8
(2)
0.6
(3)
5.0
(4)
27.0
(10
)
19.8
(1)
3.3
(3)
2
21.2
(12)
1.9
(2)
0.5
(1)
17.8
(6)
30.4
(16
)
0.2
(1)
3.5
(5)
4.8
(11)
Uzelga
2
1192.2
(16)
10(8)
24.3
(7)
179.5
(18)
188.3
(14
)
22.4
(6)
476.3
(8)
2
49.0
(6)
64.2
(3)
Alexandrinskoye
2
46.0
(8)
0.4
(5)
27.2
(15
)
3.7
(3)
26.0
(2)
24.7
(9)
1
161.8
(3)
1.3
(3)
14.6
(8)
88.2
(7)
0.5
(11)
0.8
(4)
20.8
(3)
29.3
(6)
16.2
(7)
Jusa
3
0.2
(21)
0.2
(12)
0.2
(2)
0.0
(6)
0.1
(2)
0.3
(1)
YamanKasy
1
28.8
(34)
25.4
(7)
47.0
(8)
32.1
(15
)
26.0
(6)
1/0(3)
2
530.0
(13)
73.2
(7)
465.1
(4)
1585.7
(22
)
15.0
(4)
3849.0
(6)
67
58.5
(13)
38.0
(20)
2
167.1
(20)
19.6
(8)
863.1
(7)
3194.5
(8)
102.3
(3)
21587(3)
3
78.1
(9)
818.6
(2)
54.5
(6)
3603.2
(5)
28837(4)
411.8
(1)
1652.9
(4)
27
48.5
(4)
1205.2
(10)
3
2052.1
(13)
51.9
(10)
838.0
(14)
73.3
(11)
20.4
(4)
11.5
(3)
Numberofanalysesisshowninbra
ckets.
mineralisabsent.AnalyseswerecarriedoutattheUniversityofTasmania(Ho
bart,Australia)
78 V.V. Maslennikov et al.
7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
13/34
(Table6). Possible substitutions of As and S for Te are also
inferred from our data. Extensive mixing between lllingite
and isostructural tellurides: mattagamite, melonite and
frohhbergite has been described by Ciobanu et al. (2008).
Te-rich cobaltite-like mineral Co(S,AsTe)2 (Fig. 10d).
This mineral occurs as relics of small pink cubic crystals
included in native tellurium. Commonly, grains of the
cobaltite-like mineral are corroded and replaced by other
tellurides, making their analysis by a microprobe virtually
impossible. Contents of Te in the mineral are up to 12-15 wt.
%. The calculated formula is Co1.0(As0.7Te0.2)S1.1. Some of
the high grades of Te are, probably, caused by tellurides and
native tellurium micro-inclusions. Rare homogenous areas
within this mineral, as observed in back-scattered SEM
images, were used for analysis, revealing minor amounts
of Cu, Fe, Zn, and Sb (Table 6). Their small size prevents
any crystallographic studies to determine the structure of
this mineral. The mineral merits further investigations.Te-containing gl aucodot (C o0.48 Fe0.57Cu 0.12)1.12
(As1.14Te0.02)1.16S (Table 6). Small white grains (< 5 m) have
been found in chalcopyrite-rich chimneys of types 1 and 2
in the Saphyanovskoye deposit. Glaucodot is commonly
associated with hessite and the late-formed tennantite and
tetrahedrite. High Fe contents may be due to isomorphic
series of allocrasite-glaucodot-arsenopyrite. Some grains
contain elevated Cu (411 wt. %) suggesting isomorphism
between glaucodot and lautite (CuAsS) series in the micro-
inclusions of tennantite. The elevated contents of Te (0.6
1.4 wt. %) and Ag (0.21.5 wt. %) may be due to either
substitution of Te for As, or micro-inclusions of hessite.
Pb-, Bi- and Pb-Bi tellurides and related minerals
Altaite (PbTe) is by far the most common telluride present,
usually in the form of dispersed 2-3 m grains. Larger
grains (up to 2 mm) are found adjacent to later galena in
the narrow part of zone B in type 2 chimneys from the
Yaman-Kasy and Molodezhnoye deposits (Fig. 10a, d). In
conduits of type 3 chimneys from the Oktyabrskoye deposit,
altaite occurs in sphalerite as intergrowths with hessite and
galena. Successive overgrowths and replacement of altaite
by sttzite-hessite, native tellurium and galena are common
(Fig.7d). The altaite is slightly non-stoichiometric, containing
an excess of Te. Other trace elements in altaite include Sb and
Ag (Table 4), with the likely substitution2b2+Ag1+ + Sb3+.
Altaite has high concentrations of Au, Bi and Ag. This is
consistent with published data, where altaite was also identi-
fied as a Au carrier (Ciobanu et al. 2009b; Vikentyev2006).
High concentrations of Co and As are due to micro-inclusions
of the cobaltite-like mineral.
Tellurobismuthite (Bi2Te3). Pink-white platty ctystals of
tellurobismuthite (Fig. 10b) occur in the outer and inner
parts of zone B within the chalcopyrite-rich chimneys of
types 1 and 2 in the Yaman-Kasy and Valentorskoye depos-
its (Fig.7a). Tellurobismuthite contains no S (Table 7), and
is similar to occurrences of this mineral in both pyrrhotite
and chalcopyrite-pyrite ores of Uralian type VMS deposits
(Sibai, Uchaly), which contrasts with bismuth sulfotellurides
found in galena-sphalerite-rich ores of the Baimak type VMS
deposits (Moloshag et al.2002). An excess of Te is noted in
the tellurobismuthite measured here as compared with
the theoretical formula. In the quartz-pyrite-chalcopyrite
chimneys from the Yaman-Kay deposit, Sb contents reach 7.1
Fig. 10 Reflected light photomicrographs of tellurium mineralization
in the chimneys from the Yaman-Kasy (ad, g, h), Valentorskoye (e),
Oktyabrskoye (f) deposits. a coloradoite (Cld) in association with
altaite (Alt) and frohbergite (Frb) in chalcopyrite (Cp);b tellurobis-
muthite (Tbs) at the boundary of the chalcopyrite (Cp) wall with the
sphalerite (Sl) channel; c sylvanite (Syl) twins with chalcopyrite (Cp)
in the sphalerite (Sl) matrix; d telluride mineralization (volynskite (Vol),
altaite (Alt), hessite (Hs), cobaltite (Cob), native tellurium (Te)) in asso-
ciation with sulfides (galena (Gn), marcasite (Mrc), chalcopyrite (Cp) and
sphalerite (Sl)) and quartz (Qz); e hessite (Hs) in association with
tellurobismuthite (Tbs) or kochkarite-like minerals, galena (Gn) and gold
(Au);fnative gold (Au) with hessite (Hs), tetrahedrite (Td) and galena
(Gn)in sphalerite (Sl); g crystals of goldfieldite (Gld) in quartz (Qz); h
myrmekitic intergrowths of native tellurium (Te) and silver thiotellurite
sulphosalt (Sfs)
Tellurium-bearing minerals in zoned sulfide chimneys 79
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
14/34
wt. %, where it substitutes for bismuth. Measured Sb and Bi
contents are consistent with experimental data for ternary
system BiSbTe (Caillat et al. 1992). Elevated contents of
Cu, S and Fe (Table 7) are likely due to analytical overlapcaused by the small grain size.(Table8)
Kochkarite-like ISS(Ag-Pb-Bi-Sb-Te intermediate solid
solution) occurs in chalcopyrite of zone B of pyrite-sphalerite-
chalcopyrite chimneys in the Valentorskoye deposit. Silver-
white platy crystals of these minerals are associated with sphal-
erite, hessite, galena and native gold, but not with altaite
(Fig.10e). The values of Pb are highly varied in the minerals
(Table 7). Substitution of minor Pb for Bi is widespread
throughout the group of Bi-tellurides (Cook et al. 2007b). The
phases can be considered as members of the alexite group
(Cook et al.2007a). However the most of compiled results of
analyses display the continuous compositional range from tel-
lurobismuthite to ruckligeite, not overlapping with the tsumoiteand tetradymite-aleksite ranges (Fig.11a, b). Contents of S and
Se are also low in the kochkarite-like minerals.
The most varieties of the kochkarite-like minerals have
Te contents within 5659 at. %. Some of those are probably
akin to the synthetic layered compounds with formula
PbBi6Te10 and PbBi8Te13. The series of structurally related
compounds, in close compositional proximity to one anoth-
er, can be potentially stacked in a disordered manner. These
c o m p o u n d s m a y b e l o n g t o a h o m o l o g o u s s e r i e s
Table 4 Chemical composition of tellurides from the low-sulphidation assemblages in the Type 2 and 3 chimneys from the Urals VMS
deposits (wt. %)
Frohbergite
N D Ag Te Sb Fe Co Se Tl Pd Total Formula
1 Y 82.17 0.59 12.66 4.97 0.25 100.64 (Fe0.69Co0.26)0.95(Te1.98Se0.01Sb0.01)2
2 81.70 0.62 12.99 4.49 0.19 99.99 (Fe0.72Co0.23)0.95(Te1.97Se0.01Sb0.02)2
3 81.82 0.68 12.78 4.98 0.22 100.48 (Fe0.70Co0.26)0.96(Te1.97Se0.01Sb0.02)2
4 81.87 0.64 13.32 4.23 0.19 100.25 (Fe0.73Co0.22)0.95(Te1.97Se0.01Sb0.02)2
5 81.96 17.98 99.94 Fe1.00Te2.00
6 82.04 17.86 99.90 Fe1.00Te2.00
7 81.82 18.09 99.91 Fe1.01Te2.00
Coloradoite
N D Ag Te Sb Hg Bi Se Tl Pd Total Formula
8 Y 39.82 59.00 0.44 0.30 99.56 (Hg0.94Tl0.03Pd0.01)0.98Te1
9 39.94 60.13 0.54 0.16 100.77 (Hg0.96Tl0.04Pd0.01)1.01Te1
10 39.80 61.04 0.39 101.14 (Hg0.98Pd0.01)0.99Te1
11 0.07 40.78 0.55 56.88 2.13 0.09 100.50 (Hg0.87Bi0.03)0.90(Te0.99Sb0.01)1
12 0.16 37.86 0.32 61.84 0.10 0.08 100.36 Hg1.03(Te0.99Sb0.01)1
13 U
38.28
61.13
99.41 Hg1.02Te114 38.97 60.91 99.88 Hg0.99Te1
15 38.53 60.83 99.36 Hg1.00Te1
Altaite
N D Ag Te Sb Pb Co Se Tl Pd Total Formula
16 Y 0.34 38.09 0.30 60.22 99.20 (Pb0.97Ag0.01)0.98(Te0.99Sb0.01)1
17 0.34 39.01 0.24 60.44 0.08 100.12 (Pb0.95Ag0.01)0.96(Te0.99Sb0.01)1
18 0.44 37.76 0.27 61.25 99.94 (Pb0.99Ag0.01)1.00(Te0.99Sb0.01)1
19 0.19 38.12 0.00 61.03 99.34 (Pb0.99Ag0.01)1.00Te1.00
20 M 37.54 62.39 99.93 Pb1.02Te1
21 37.72 62.25 99.97 Pb1.02Te1
22 38.14 61.64 99.78 Pb1.01Te1
23 O
38.12
61.18
99.30 Pb0.99Te1
24 1.87 38.77 59.02 99.65 (Pb0.94Ag0.03)0.97Te1
25 37.36 62.42 99.78 Pb1.03Te1
D VMS deposits: Y Yaman-Kasy; U Uzelga; M Molodezhnoye; O Oktyabrskoye; V Valentorskoye. element has not been analysed.
Analyses were carried out: 14, 11, 12, 16, 17 by JEOL JXA 8900 RL (the University of Tasmania, Hobart, Australia); 57, 1315, 2025 inby
REMMA-2 M SEM (the Institute of Mineralogy of UB RAS), 810 inby Camebax SX50 (NHM, London, England); 1819 in JEOL JXA
8900 RL (Freiberg Mining Academy, Freiberg, Germany)
80 V.V. Maslennikov et al.
http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-http://-/?-7/23/2019 Te-Zn-Cu Sulfuros Masivos Rusia
15/34
Table5
Traceelementconcentratio
ns(ppm)inaccessorymineralsfromthepa
leo-hydrothermalchimneys(LA-ICP-MS)
N
Minerals
Te
Bi
Ag
Au
Fe
Pb
Cu
Zn
As
Se
V
1
Tellurobismuthite(9)
mean
459409
490000
4709
2.5
1
4406
30568
4640
375
2.5
4
5189
31.2
4
max
495619
542000
7491
8.0
7
21639
48294
23984
1976
6.2
1
5971
103.7
0
min
404833
431000
3014
0.3
3
64
16745
25
0
0.5
2
4358
0.2
3
2
Sylvanite(2)
621000
6.9
7
130536
217269
13444
10
16767
136
0.2
8