GeolCarp_Vol68_No4_366

GEOLOGICA CARPATHICA

, AUGUST 2017, 68, 4, 366 – 381

doi: 10.1515/geoca-2017-0025

www.geologicacarpathica.com

Bi-sulphotellurides associated with Pb – Bi – (Sb ± Ag, Cu, Fe)

sulphosalts: an example from the Stan Terg deposit in Kosovo

JOANNA KOŁODZIEJCZYK



, JAROSLAV PRŠEK

, PANAGIOTIS CH. VOUDOURIS

and VASILIOS MELFOS

AGH University of Science and Technology, Faculty of Geology, Geophysics and Environmental Protection, Department of Economic

Geology, al. Mickiewicza 30, 30-059 Kraków, Poland;



asia.office@wp.pl (J.K.), prsek@geol.agh.edu.pl (J.P.)

Department of Mineralogy-Petrology, National and Kapodistrian University of Athens, Athens 15784, Greece; voudouris@geol.uoa.gr

Department of Mineralogy, Petrology and Economic Geology, Aristotle University of Thessaloniki, Thessaloniki 54124, Greece;

melfosv@geo.auth.gr

(Manuscript received December 26, 2016; accepted in revised form March 15, 2017)

Abstract: New mineralogical and mineral-chemical data from the Stan Terg deposit, Kosovo, revealed the presence of

abundant Bi-sulphotellurides associated with Bi- and Sb-sulphosalts and galena in pyrite–pyrrhotite-rich skarn-free ore

bodies (ores without skarn minerals). The Bi-bearing association comprises Bi-sulphotellurides (joséite-A, joséite-B,

unnamed phase A with a chemical formula close to (Bi,Pb)

(TeS)

, unnamed phase B with a chemical composition close

to (Bi,Pb)

2.5

1.5

), ikunolite, cosalite, Sb-lillianite, members of the kobellite series and Bi-jamesonite. Compositional

trends of the Bi-sulphotellurides suggest lattice-scale incorporation of Bi–(Pb)-rich module and/or admixture with

submicroscopic PbS layers in modulated structures, or complicated Bi–Te substitution. Cosalite is characterized by high

Sb (max. 3.94 apfu), and low Cu and Ag (up to 0.72 apfu of Cu+Ag). Jamesonite from this mineralization has elevated

Bi content, from 0.85 to 2.30 apfu. The negligible content of Au and Ag in the Bi-sulphotellurides, the low content of Ag

in Bi-sulphosalts, together with the lack of Au–Ag bearing phases in the mineralization, indicate either ore deposition

from fluid(s) depleted in precious metals, or physico-chemical conditions of ore formation preventing Au and Ag

precipitation at the deposit site. The temperature of initial mineralization may have exceeded 400 ºC as suggested by the

lamellar exsolution textures observed in lillianite, which indicate breakdown textures from decomposition of high-

temperature initial crystals. Non-stoichiometric phases among the Bi-sulphosalts and sulphotellurides studied at Stan

Terg reflect modulated growth processes in a metasomatic environment.

Keywords: Kosovo, Stan Terg, Bi-tellurides, tetradymite group minerals, Sb-cosalite, Sb-lillianite, kobellite homologous

series.

Introduction

Bismuth sulphotellurides are common mineral phases occur-

ring in high-temperature associations with Bi-sulphosalts and

Au mineralization in Pb–Zn skarn deposits (Cook et al. 2007a),

VHMS deposits (Vikentyev 2006), orogenic Au deposits

(Bowell et al. 1990; Ciobanu et al. 2010), Au-bearing quartz-

veins in intrusion-related systems (Cepedal et al. 2013), nickel

mineralization in greenstone belts (Groves & Hall 1978),

and porphyry-epithermal systems (Cook & Ciobanu 2004;

Melnikov et al. 2009;

Pršek & Peterec 2008;

Plotinskaya et al.

2009). Tellurium mineralization, together with Bi, is com-

monly linked to Au occurrences (Ciobanu et al. 2009a; Cook

et al. 2009).

Bismuth sulphotellurides are stable over a wide temperature

interval and their composition reflects the geochemical

characteristics of the mineralization environment (Melnikov

et al. 2009).

The tetradymite group comprises 19 mineral species and

several unknown phases which can be ordered into the follo-

wing subspecies: Bi

–Bi

, Bi

–Bi

and BiTe–BiSe–BiS (Cook et al. 2007a). These minerals

have usually rhombohedral- or trigonal-layered structures and

limited variation in composition. Minor Pb ↔ Bi substitution

is widespread throughout the group, especially in the

–Bi

subgroup.

The precise identification of sulphotelluride phases is not

easy because they are commonly intergrown with each

other on the submicroscopic scale. Due to the small size

of mineral aggregates, X-ray diffraction structural data

cannot be obtained, hence many unknown sulphotelluride

phases identified by EPMA, could not be thoroughly

characterized.

At the Stan Terg Pb–Zn(–Ag–Bi) deposit, within the Trepça

Mineral Belt, in Kosovo, the Bi-bearing sulphosalts and

chalcogenides, ikunolite, babkinite, joséite-A, izoklakeite,

cannizzarite, lillianite-gustavite and heyrovskýite, were

previously described in samples from galena-rich skarn mine-

ralization (e.g., orebodies No. 140 and 149), and from arseno-

pyrite-rich skarn-free mineralization (corridor walls in the

southern part of the X

horizon) (Kołodziejczyk et al. 2015).

Kołodziejczyk et al. (2015) suggested that the bismuth- bearing

phases at Stan Terg were formed during the retrograde evolu-

tion of the hydrothermal system under generally low-sulphi-

dation and reduced fluid states in the temperature range from

350 to 250 °C.

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Bi-SULFOTELLURIDES AND SULFOSALTS FROM THE STAN TERG DEPOSIT, KOSOVO

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This study provides detailed mineralogical and geochemical

data concerning new sulphotellurides found in association

with Bi-sulphosalts in the Stan Terg deposit. Electron micro-

probe data are provided for all phases identified, and their

physico-chemical conditions of formation are discussed in

comparison with similar assemblages elsewhere.

Geological setting

Stan Terg, the largest known Pb–Zn deposit in Kosovo, hosts

polymetallic mineralization with abundant assemblages con-

taining Bi-, Sb-, Ag- and Sn-bearing minerals, and average ore

grades at 3.65 % Pb, 3.55% Zn, and Bi, Ag and Sn as signifi-

cant by-products (average 87 g/t Ag, 100 g/t Bi, and 30 g/t Sn).

The mineralization is related to the Tertiary (Oligocene–

Miocene) magmatic activity that took place within the Trepça

Mineral Belt, which is a part of the Vardar suture zone, stret-

ching from the north to the south through the Balkan Peninsula,

in southeastern Europe (Hyseni et al. 2010; Strmić Palinkaš et

al. 2013). The significance of the Trepça Mineral belt has been

confirmed by many authors who have described different

types of Pb–Zn mineralization such as skarn, hydrothermal

replacement, and vein mineralization considered to be con-

trolled primarily by faults (e.g., Janković 1995).

The area around the Stan Terg deposit is composed of

Triassic sedimentary and volcanoclastic rocks, upper Triassic

carbonates, ophiolite mélange with Jurassic ultrabasic rocks

and serpentinites, and Cretaceous series of clastics, serpen-

tinites, volcanics and volcanoclastic rocks of basaltic compo-

sition and carbonates (Fig. 1A). The area is covered by Tertiary

volcanics, like lavas, sub-volcanic intrusives and pyroclastic

rocks, dominated by andesite, trachyte and latite composition

(Hyseni et al. 2010). The mineralization in the Stan Terg

deposit is related to post-collisional magmatism (Féraud &

Deschamps 2009; Strmić Palinkaš et al. 2013), and the nearest

magmatic rocks of calc-alkaline composition that are exposed

on the surface are in the Kopaonik Massif, in the northern part

of Kosovo.

Ore mineralization

The ore mineralization is hosted mostly within Triassic car-

bonates (marbles) in several elongated orebodies (eleven main

orebodies) that plunge parallel and commonly join or split

forming a type of large stockwork. The shape of orebodies is

controlled by an anticline structure with carbonates in the core

and shielded by sericite schists in the external part. The hydro-

thermal fluid transport was controlled by faults, fissures and

palaeo-karst cavities. Until today, ore was excavated from 11

mining horizons, but the final depth has not been documented

(Féraud & Deschamps 2009). There is also a volcanic conduit

with phreatomagmatic breccias in the central part of the

deposit (Féraud & Deschamps 2009; Strmić Palinkaš et al.

2013) that stretch parallel to the orebodies. Parts of the

orebodies are related to skarn mineralization, parts are skarn-

free carbonate-replacements (e.g., mantos-type), and signifi-

cant ore precipitated as karst fillings. Karst fillings originated

by the corrosive action of the metalliferous hydrothermal solu-

tions dissolving the limestones (Forgan 1950; Schumacher

1950; Féraud et al. 2007).

The ore mineralization is dominated by galena, sphalerite,

pyrite, pyrrhotite, arsenopyrite, with minor chalcopyrite, tetra-

hedrite, Sn-minerals, Bi-minerals, Ag-minerals and native

elements (Kołodziejczyk et al. 2015, 2016 a,b). The skarn

alteration (garnet, hedenbergite, ilvaite and actinolite, magne-

tite) is present near the central volcanic conduit, but also in the

distal parts of the deposit (Dangić 1993). The previously

described Bi-sulphosalt mineralization is hosted in both skarn-

and skarn-free orebodies and is considered to represent

a single stage of mineral precipitation (Kołodziejczyk et al.

2015). The skarn orebodies usually contain a silicate para-

genesis with base metal sulphides and Bi-minerals, whereas

skarn-free orebodies with Bi-mineralization occur in the form

of brecciated veins. Both mineralization types occur at the

same depth level, close to the central breccia-pipe. Strmić

Palinkaš et al. (2013) recognized a prograde magmatic stage

(with precipitation of pyroxene and garnet), and following

retrograde skarn and a hydrothermal stage dominated by

ilvaite, magnetite, Pb-, Zn- and Fe-sulphides, quartz and

carbonates. According to their work, the source of hydro-

thermal fluids is magmatic, and the fluid was partially

mixed with meteoric waters during infiltration in the country

rocks.

Sampling and methodology

The studied Bi–Pb–Sb–S–Te-bearing mineral assemblages

were found in ten samples from recently developed orebodies;

No. 141 and 140 in the X

horizon of the Stan Terg mine

(Fig. 1B).

The chemical composition of the sulphotellurides and

sulpho

salts were determined using a JEOL JXA-8230

Superprobe electron probe microanalyser (EPMA) in the

Critical Elements Laboratory at the Faculty of Geology,

Geophysics, and Environmental Protection, AGH University

of Science and Technology in Krakow. All measurements

were done on carbon-coated polished sections using the follo-

wing operating conditions: accelerating voltage 20 kV, beam

current 20 nA, and a beam diameter ~1 μm. The following

spectral lines, standards (metals and sulphides), count times

(peak and background for unknowns) were used: S (SK

, FeS

20 s, 10 s), Fe (FeK

, FeS

, 20 s, 10 s), Cu (CuK

, Cu, 20 s, 10 s),

Se (SeL

, Se, 20 s, 10 s), Ag (AgL

, Ag, 20 s, 10 s), Sb (SbL

, 20 s, 10 s), Te (TeL

, PbTe, 20 s, 10 s), Pb (PbM

, PbS,

20 s, 10 s), Mn (MnK

,, MnS, 20 s, 10 s) and Bi (BiM

, Bi, 20 s,

10 s). The typical minimum detection limits for those analy-

tical conditions were: Te (120 ppm), S (30 ppm), Pb (160 ppm),

Bi (140 ppm), Cu (50 ppm), Fe (40 ppm), Ag (40 ppm),

Sb (40 ppm), Se (80 ppm), Mn (120 ppm). Back-scattered

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Bi-SULFOTELLURIDES AND SULFOSALTS FROM THE STAN TERG DEPOSIT, KOSOVO

GEOLOGICA CARPATHICA

, 2017, 68, 4, 366 – 381

sulphosalts and with minor galena. This mineral association is

dispersed between pyrite, marcasite, and pyrrhotite crystals

hosted in a carbonate matrix (Fig. 2). Aggregates occur up to

500 μm in size, and single phases of sulphosalts recognized in

BSE images are usually around 10–20 μm, whereas sulpho-

tellurides are mostly up to 5 μm. The Bi-bearing association

studied comprises Bi-sulphotellurides (joséite-A, joséite-B,

unnamed phase A, unnamed phase B), ikunolite, cosalite,

Sb-lillianite, kobellite series members and Bi-jamesonite.

Tellurides occur as elongated inclusions in cosalite or lillia-

nite aggregates, with sizes up to 20 μm (Fig. 3 A). In part of the

inclusions, intergrowths composed of different chemical com-

positions are present, for example, phase A and phase B

(Fig. 3B), or joséite-A and joséite-B (Fig. 3 C,D). Phase A and

phase B often form intergrowths with different Te concentra-

tions in various parts of the cosalite crystals. Joséite-A and

joséite-B occur primarily as intergrowths with native bismuth

(Fig. 3 D), or with ikunolite (Fig. 3 E,F). Lillianite occurs in

aggregates with cosalite, native bismuth and tetradymite group

minerals. An important feature of lillianite from the sulphotel-

luride association is exsolution lamellae, visible as darker and

lighter phases observed with BSE imaging (Fig. 3 E). Cosalite

was found in this study in association with Bi-sulphotellurides

and other Bi-sulphosalts. It occurs as intergrowths with galena

(Fig. 3 C, E, F), or the Sb-rich lillianites and the kobellite

homologues series (Fig. 3 G, H). Jamesonite occurs as needles

or larger irregular aggregates replacing other minerals, like

galena or izoklakeite-giesenite and cosalite (Fig. 3 H).

Sulphotelluride association

Four different chemical compositions of sulphotellurides

were identified; primarily joséite-A (ideally Bi

TeS

), joséite-B

(ideally Bi

S), and two phases (of composition close to

(Bi,Pb)

(TeS)

and (Bi,Pb)

2.5

1.5

) that could not be unam-

biguously assigned to any known minerals, and are described

below as phase A, and phase B. Chemical compositions from

representative EPMA analyses are presented in Tables 1 and 2.

The range of chemical compositions of the phases recognized

are plotted in Figure 4. The EPMA data do not fall exactly on

theoretical end-member values, and are rather dispersed on the

plot.

The joséite-A EPMA data plot on a line, starting with

an ideal stoichiometric joséite-A chemical composition and

continuing in the direction of increased S, Pb, and Bi contents

(Fig. 4). The Pb content in phases assigned to the joséite-A

group are from 2.69 to 9.52 wt. %, Bi varies from 75.93 to

79.31 wt. %, Te from 7.63 to 11.83 wt. % and S from 6.39 to

7.32 wt. % (Table 1). The Ag content is up to 0.05 wt. %, Se

up to 0.15 wt. % and Sb up to 0.34 wt. %.

Joséite-B has a similar trend to joséite-A through increased

S, Pb, and Bi contents, towards the ideal Bi

TeS composition.

The Pb content in phases assigned to the joséite-B group are

up to 2.58 wt. %, Bi varies from 68.12 to 79.35 wt. %, Te from

14.92 to 24.18 wt. % and S from 2.81 to 3.94 wt. %. The Ag

content is up to 0.05 wt. %, of Se up to 0.20 wt. % and Sb up

to 0.68 wt. %. Phase A has a chemical composition between

telluronevskite and ingodite (Fig. 4). Its general structural for-

mula is (Bi,Pb)

(TeS)

. The (Bi+Pb) to (S+Te+Se) ratio is 1:1.

The scatter plot with data for Phase A and Phase B falls away

from aleksite sub-group line as was proposed by Cook et al.

(2007 b) on their figure 6 therein so we are not considering our

phases as aleksite sub-group minerals.

Compositions assigned to phase A have 5.50 –20.37 wt. % Pb,

51.71–74.55 wt. % Bi, 16.65 –22.82 wt. % Te, and 5.32–9.95

wt. % S (Table 2). Phase A contains up to 0.16 wt. % of Ag.

Fig. 2. Host rock samples for bismuth-telluride association occurring between elongated pyrite (py) crystals in the carbonate matrix (crb).

A — Sample from orebody No. 140 overgrown by coarse-grained galena (gn); B — Sample from orebody No. 141.

Fig. 3. BSE images of the sulphotelluride Bi–Sb–Pb–Te–S association. A — Cosalite (cos) aggregate with telluride minerals (white inclusions).

B — Detail of image A. Telluride inclusions composed of phases A and B. C — Aggregate of cosalite (cos) replacing galena (gn) with

tetradymite minerals: ikunolite (ikn), joséite-B (josB) and native bismuth (Bi). D — Detail of image C. Joséite-A (josA) intergrown with

joséite-B (josB) and native bismuth (Bi). E — Lillianite exsolutions. White needles with high Ag content, and darker needles with low

Ag content. Gn – galena, cos – cosalite, ikn – ikunolite, josB – joséite-B. F — Cosalite (cos) and native bismuth (Bi) replacing galena (gn).

josA – joséite-A, ikn – ikunolite, L – lillianite. G — Aggregate composed of kobellite-tintinaite (kob), izoklakeite-giessenite (izo),

cosalite (cos), and galena (gn). H — jamesonite (jm) replacing cosalite (cos) and izoklakeite-giessenite (izo). Kob – kobellite-tintinaite.

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Bi-SULFOTELLURIDES AND SULFOSALTS FROM THE STAN TERG DEPOSIT, KOSOVO

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Phase B has a chemical composition close to

(Bi,Pb)

2.5

1.5

. The (Bi+Pb) to (S+Te+Se) ratio is 2.5:3, and

this telluride has the highest Te content, that is in the range

between 25.87 and 29.33 wt. % (Table 2). Lead varies between

8.80 –10.19 wt. %, Bi between 55.95 and 61.44 wt. %, and

S between 5.85 and 6.28 wt. %.

Ikunolite

Ikunolite (ideally Bi

(S,Se)

) is a tetradymite-group mineral

previously described in Stan Terg in association with other

Bi-minerals and joséite-A (Kołodziejczyk et al. 2015).

Previous analyses indicated

a good correlation between Pb and

Bi in ikunolite, babkinite

and the intermediate phases, sug-

gesting a possible ikunolite-

babkinite solid solution, with very

limited Se for S substitution

(Kołodziejczyk et al. 2015).

Ikunolite-babkinite solid solutions

revealed up to 0.25 wt. % Te and

up to 0.3 wt. % Ag (Kołodziejczyk

et al. 2015).

Ikunolite within the sulphotel-

luride association (this study),

occurs mostly as intergrowths

with the above described sulpho-

tellurides and with lillianite, cosa-

lite, native bismuth, and galena.

Representative EPMA analyses of

ikunolite are presented in Table 1.

Its Pb content varies between 0.99

and 23.40 wt. %, and there is

a positive correlation trend towards

the babkinite composition, how-

ever only up to 0.9 apfu of Pb.

The ikunolite contains Ag up to

0.13 wt. %, Sb up to 0.11 wt. %,

and up to 1.22 wt. % Te. Selenium

up to 0.15 wt. % was detected in

some analyses. Ikunolite has

a composition similar to ikunolite

from the skarn-hosted and skarn-

free mineral association (e.g.

Kołodziejczyk et al. 2015), with

Pb concentrations up to 23 wt. %

(for intermediate ikunolite-babki-

nite phases).

Cosalite

Cosalite was previously des cri-

bed from Stan Terg by Terzić et al.

(1974, 1975), with a single EPMA

analysis indicating chemi cal

compo sition close to ideal, with 0.27 apfu of Sb, and up to

0.01 apfu of Ag.

Representative EPMA analyses of cosalite, together with

analyses for coexisting galena, are presented in the Table 3.

Cosalite has up to 0.72 apfu of Cu+Ag (1.50 wt. %), and up

to 3.94 apfu of Sb (13.57 wt. %), thus resulting in a shift of

chemical composition of the Stan Terg cosalite towards

increased Sb content (Fig. 5). Binary plots with compositional

data for Stan Terg cosalite for Cu+Ag, and Pb, Bi, Bi+Sb

are presented in Figure 6. There is a good correlation

between Sb and Bi over a wide range of Sb/(Sb+Bi) ratios

(Fig. 6D).

0.77

1.08

4.28

10.22

7.34

3.79

0.61

1.55

0.19

0.71

0.29

0.32 <MDL

0.05

0.04

0.17

0.02

0.07

0.12

0.03

0.47

0.03

0.03 <MDL <MDL <MDL <MDL <MDL <MDL <MDL

0.03

0.01 <MDL

0.04

0.13

0.08

0.01 <MDL

0.02

0.01 <MDL

0.03 <MDL

0.05

0.03 <MDL

0.04

0.09

0.22

0.25

0.37

0.36

0.46

0.42

0.46

89.37

89.54

86.42

79.8

78.21

79.49

75.93

75.89

76.87

76.21

76.78

0.83

1.16

0.16

0.74

7.76

10.47

21.87

20.69

21.12

21.32

0.11

0.10

0.04 <MDL <MDL

0.07 <MDL <MDL

0.09 <MDL

0.01

10.04

10.21

10.19

10.34

6.91

6.74

2.89

3.07

3.04

3.03

TOTAL

101.54 102.22 101.26 101.24 100.61 100.85 101.75 101.68 101.86 101.97 101.97

Chemical formula based on sum of 7 atoms

0.03

0.05

0.19

0.45

0.36

0.18

0.03

0.08

0.01

0.04

0.02

0.05

–

0.01

0.03

0.00

0.01

0.02

0.01

0.09

0.01

0.00

–

0.00

–

0.00

0.01

0.00

–

0.00

–

0.00

–

0.01

0.00

–

0.00

0.01

0.02

0.03

0.04

3.94

3.93

3.83

3.51

3.79

3.83

4.02

4.01

4.05

3.99

4.05

0.06

0.08

0.01

0.05

0.62

0.83

1.90

1.79

1.82

1.81

1.84

0.01

0.00

–

0.01

–

0.01

–

0.00

2.89

2.92

2.94

2.97

2.19

2.12

1.00

1.06

1.05

1.03

1.04

Notes: <MDL = below the minimum detection limit

10.31

12.01

10.41

17.11

9.02

8.80

8.32

8.80

0.02

0.06

0.04

0.36

0.02

0.12

<MDL

0.01

<MDL

0.01

<MDL

0.01

0.05

0.02

0.09

0.04

<MDL

0.01

<MDL

0.14

0.20

0.40

0.23

0.21

0.19

0.23

69.27

62.34

63.91

56.41

55.95

59.32

59.54

56.32

13.88

18.60

18.67

17.86

28.75

26.48

25.68

29.33

0.03

<MDL

0.09

0.04

<MDL

0.05

<MDL

0.11

6.73

7.06

6.73

8.11

5.86

5.96

5.93

5.79

TOTAL

100.18

100.33

100.08

100.38

99.87

100.85

99.69

100.71

Chemical formula based on sum of 2 cations

Chemical formula based on sum of 2.5 cations

0.26

0.33

0.28

0.47

0.35

0.33

0.31

0.34

0.00

0.01

0.00

0.04

0.00

–

0.00

–

0.00

–

0.00

0.01

0.00

–

0.00

–

0.01

0.02

0.01

0.02

1.74

1.67

1.72

1.53

2.15

2.17

2.19

2.16

0.57

0.82

0.79

1.81

1.59

1.55

1.84

0.00

–

0.01

0.00

–

0.01

–

0.01

1.10

1.24

1.18

1.44

1.47

1.42

1.45

Notes: <MDL = below the minimum detection limit

Table 1: Representative EPMA analyses and atomic proportions for tetradymite group minerals from

the sulphotelluride association: ikunolite (1–4), joséite-A (5–6), joséite-B (7–11) in the Stan Terg

deposit.

Table 2: EPMA analyses of phase A (1–4) and phase B (5–8) from the sulphotelluride association in

the Stan Terg deposit.

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, 2017, 68, 4, 366 – 381

Sb-rich lillianite

Lillianite (N = 4) and heyrovskite

(N = 7), two members of the lillianite

homologous series, were recently

reported at the Stan Terg deposit in

association with other Bi-sulphosalts,

galena and arsenopyrite (Koło-

dziejczyk et al. 2015). They contain

up to 0.2 wt. % of Sb.

In contrast, lillianite accompany-

ing the Bi-sulphotellurides has a dif-

ferent chemical composition with

significantly higher Sb content (up to

11.50 wt. %), and also a higher Ag

content (up to 5.10 wt. %). This

Sb-rich lillianite has been found in

the samples from the orebody 141, as

aggregates intergrown with galena,

native bismuth, cosalite, and tet-

radymite group minerals.

40.00

40.58

40.65

40.21

41.67

43.49

84.77

85.47

84.89

0.59

0.21

0.25

0.27

0.26

0.64

0.03

0.05

0.32

0.16

0.17

0.14

0.16

0.98

<MDL

0.02

0.89

0.48

0.44

0.65

0.67

0.52

0.58

0.18

0.32

0.41

3.47

3.89

6.14

7.61

13.57

0.03

<MDL

41.42

37.47

37.21

34.40

31.79

22.34

2.52

1.31

1.51

<MDL

0.14

0.06

0.16

0.21

0.00

0.01

<MDL

0.01

0.04

0.07

0.03

<MDL

0.13

0.04

0.03

0.14

<MDL

16.03

16.70

16.65

16.99

17.21

18.13

13.50

13.05

13.42

TOTAL

99.70

99.28

99.35

98.96

99.71

101.47

100.18

100.22

Chemical formula based on anions = 20

Chemical formula based on 2 atoms

7.52

7.51

7.55

7.33

7.48

7.42

0.96

0.98

0.97

0.42

0.15

0.17

0.19

0.18

0.40

0.00

0.21

0.10

0.11

0.09

0.10

0.55

–

0.00

0.33

0.17

0.16

0.23

0.17

0.01

0.00

0.01

0.13

1.09

1.07

1.90

2.32

3.94

0.00

–

7.92

6.88

6.85

6.21

5.66

3.78

0.03

0.01

0.02

–

0.01

0.04

0.11

0.14

0.00

0.12

–

0.00

0.01

0.02

0.01

–

0.04

0.01

0.00

–

19.99

19.98

19.99

20.00

19.96

19.99

0.98

0.97

0.99

Notes: <MDL = below the minimum detection limit, Se was below the minimum detection limit in all analyses

Table 3: Representative EPMA analyses and atomic proportions for cosalite (1–6) and coexisting

galena (7–9) from Stan Terg.

Fig. 4. Ternary plot Bi+Pb+Sb vs S+Se vs Te of Bi-sulphotelluride minerals from the Stan Terg mine. Open circles: minerals ideal end member

chemical compositions; solid black symbols: chemical compositions of minerals from the Stan Terg deposit.

Pb+Bi+Sb

S+Se

bismuthinite

telluronevskite

Bi S

Bi TeS

Bi Te

(Pb,Bi) Te S

2.5

1.5

(Pb,Bi) Te S

saddlebackite

tetradymite

tsumoite

pilsenite

rucklidgeite

tellurobismutite

sulphotsumoite

joseite-B

joseite-A

baksanite

ingodite

JOSEITE-A

JOSEITE-B

PHASE-A

PHASE-B

ikunolite

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Representative EPMA data are presented in Table 4. For all

ana lysed grains the N number was calculated with values

around 4 (e.g., 3.70 – 4.14), which means the only member

of the lillianite homologous series present in the association

is lillianite, 4L. The molar percentage of the gustavite

member ranges between 8.08 and 55.60 mol. %, whereas

the silver content in apfu (x) ranges between 0.08 and 0.51

(Fig. 5).

By comparing the chemical composition of exsolution

lamellae in lillianite we conclude that the lighter phases are

described as

3.76

18.75

, with x value = 0.17, whereas the darker

zones are enriched in Ag, and their composition is around

3.76

59.93

, with x = 0.47 (both measured with an e lectron beam

diameter below 1 μm). One analysis with a 4 μm electron

beam, could be assigned to an unexsolved phase that was

around

3.83

26.28

, with x = 0.24.

X-ray maps (Fig. 7) show a lillia nite aggregate from the

sulphotelluride association, partly replaced by galena,

ikunolite, native bismuth, and Bi-sulpho

tellurides

(joséite-A, joséite-B). Copper and Pb distribution are

uniform throughout the lillianite aggregates, whereas Ag and

Sb are slightly increased at the edges. Sulphotellurides are

intergrown with ikunolite, or occur as inclusions in galena or

lillianite.

Kobellite homologous series

Recently, the presence of izoklakeite-giessenite members of

the kobellite homologous series in the Stan Terg deposit was

reported by Kolodziejczyk et al. (2015). In the sulphotelluride

asso ciation (samples from 140 and 141 orebodies), phases that

represent both members, for example, izoklakeite - gies se nite

(N=4), as well as kobellite-tintinaite series (N=2) were identi-

fied. However, in this association izoklakeite- giessenite

phases are dominant.

Kobellite homologous series phases occur in the sulpho-

telluride association together with Bi-rich jamesonite, Sb-

cosalite (up to Sb 3.94 apfu), and minor galena

(Fig. 3G,H). The chemical composition of these minerals is

presented in Table 5 and in Figure 8.

An almost ideal Bi ↔ Sb substitution trend is visible in both

series (Fig. 8A). The Sb/(Sb+Bi) ratio is 0.47– 0.51 in the

kobellite- tintinaite series and 0.31– 0.51 in the izo klakeite-

giessenite series. The Ag content is insignificant, and

Bi+Sb

Cu+Ag

Gustavite

Galenobismutite

Cannizzarite

Cosalite

Lillianite N=4

Heyrovskyite N=7

Matildite

Bismuthinite

Treasurite

Vikingite

Eskimoite

Ourayite

Bi-minerals - this study

Bi-minerals (Kołodziejczyk et al..2015)

Theoretical formulae

N=5

N=5.5

N=6

N=8

N=9

N=10

N=11

Fig. 5. Ternary plot Cu+Ag vs Bi+Sb vs Pb of bismuth sulphosalts — new data and previously described phases in the Stan Terg mine.

374

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1.6

1.2

0.8

0.4

19.5

20.5

21 21.5

Pb (at %)

Cu+Ag (at %)

1.6

1.2

0.8

0.4

Cu+Ag (at %)

1.6

1.2

0.8

0.4

Cu+Ag (at %)

Bi+Sb (at %)

Bi (at %)

Sb (at %)

corresponds to 0.1 apfu and 0.5

apfu on average in both series,

respectively.

Bi-rich jamesonite

Jamesonite from the Stan Terg

deposit was found in samples

from the 140 orebody. Repre-

sentative EPMA data are presen-

ted in Table 6. Chemical

com po sition data indicates that

the Bi content in all phases mea-

sured reaches up to 21 wt. %,

which corresponds to 0.85 to 2.30

apfu in the chemical formula.

Discussion

The Bi–Pb–Sb–S–Te associa-

tion discussed in the present study differs from that described

pre viously by Kołodziejczyk et al. (2015) (e.g., skarn-, and

skarn-free breccias filling types), in that it is enriched in tellu-

rides. This association was found in the external parts of the

skarn ore bodies as aggregates between dispersed pyrite crys-

tals in the gangue carbonate host rock. The source of the

Bi–Pb–Sb–S–Te mineralization is likely to be the same as for

the two types described above, and the Bi-sulphotelluride

Fig. 6. Binary plots showing chemical composition of cosalite from the Stan Terg deposit. A — Cu vs Ag at. %; B — Cu+Ag vs Pb at %;

C — Cu+Ag vs Bi at. %; D — Cu+Ag vs Bi+Pb at. %.

37.86

34.66

40.52

38.75

40.53

48.67

46.04

48.48

41.35

35.02

<MDL

0.05

0.09

0.04

0.90

0.06

0.16

1.32

0.16

0.49

0.01

<MDL

0.01

<MDL

0.02

0.08

3.87

4.60

3.24

3.48

3.05

1.00

1.26

3.60

5.10

0.34

0.36

0.50

0.62

0.68

1.21

1.24

1.89

4.99

11.50

43.14

45.19

40.15

42.76

40.52

33.99

34.50

33.24

35.39

29.22

<MDL

0.01

<MDL

0.08

0.04

<MDL

0.07

<MDL

16.29

16.20

16.11

16.09

15.97

15.47

15.80

15.60

16.16

17.88

TOTAL

101.51

101.06

100.61

101.75

101.66

100.48

99.04

101.79

101.74

99.29

Chemical formula based on (Pb+Bi+Ag) = 5

2.15

1.96

2.34

2.21

2.34

2.89

2.78

2.89

2.48

2.37

2.43

2.54

2.30

2.41

2.32

2.00

2.07

1.97

2.11

1.96

0.42

0.50

0.36

0.38

0.34

0.11

0.15

0.14

0.41

0.66

5.98

5.93

6.01

5.92

5.96

5.93

6.18

6.01

6.26

7.82

3.93

3.86

4.08

3.83

3.94

4.11

4,00

4.16

4.01

3.82

mol%

42.75

51.90

34.83

39.62

33.92

10.83

14.26

13.24

37.52

55.60

0.41

0.48

0.36

0.33

0.11

0.14

0.38

0.51

Notes: <MDL = below the minimum detection limit

Table 4: Representative EPMA analyses and atomic proportions for Sb-rich lillianite from sulpho-

telluride association in the Stan Terg deposit.

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KOŁODZIEJCZYK, PRŠEK, VOUDOURIS and MELFOS

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, 2017, 68, 4, 366 – 381

could be disordered members of

the tsumoite – ingodite – nevskite

series. They do not rule out, how-

ever, the possibility of stable min-

erals with this stoichiometry.

Our compositional data for

joséite-A and joséite-B, trend in

the direction of the “protojoseite

line”, marked according to its

stoichiometric formula of

(Te,S)

, indicating a wide com-

positional range of Te and S in

this phase (Fig. 9A). Some of the

data plot directly on this line.

Protojoseite remains a question-

able mineral species (e.g., Jambor

1984) and its stoichiometry was

reported as 3:2 and 4:3, or the

phase was suggested to be a non-

stoichiometric joséite-B or

joséite-A (Cook et al. 2007a).

Zav’yalov & Begizov (1983) sug-

gested a narrow

compositional

field for protojoseite with the

general formula Bi

3+ x

1− x − y

1+ y

where

−0.02 < x < 0.14

and

−0.05 < y < 0.17, which may explain the Bi: (Te + S) variations

that were observed.

Results similar to those obtained in the present study, for

coexisting joséite-B and “protojoseite”, were reported by

Zav’yalov & Begizov (1983), and later by Cook et al. (2007a).

However, in these studies, the compositional data differ

noticeably for both species, and the results do not overlap with

fields for ideal stoichiometric joséite-A and joséite-B.

Compositions which are apparently non-stoichiometric can

be readily interpreted in terms of (disordered or ordered)

finest-scale intergrowths, as described by Cook et al. (2007a,b):

The “PbS sublayers” approach is supported by the three visible

trends on the Pb+Bi+Sb vs S+Se vs Te diagram (Fig. 9 B):

from Bi

– to joséite-B; 2

from Bi

– joséite-A –

sulphotsumoite – to tellurobismutite; and 3

from ikunolite –

phase A with formula (Bi,Pb)

(TeS)

– phase B with for mula

(Bi,Pb)

2.5

1.5

– to tetra dymite. Those lines can support the

admixture of tellurides with submicroscopic intergrown layers

of PbS, so the analyses fall between the phases mentioned

above on that diagram.

Although unnamed Phases A and B plot away from the

aleksite sub-group line (e.g. Cook et al. 2007a) and thus can-

not be explained in terms of aleksite sub-group phases, the

observed compositions could be alternatively, attributed to

submicroscopic intergrowths of tetradymite units with Pb–Bi

sulphotellurides.

Finally, lattice-scale intergrowths between members of the

tetradymite group (e.g. conside

ration of Bi–Pb modules

approach), similar to those described by Ciobanu et al. (2009b)

could also explain the composition of unnamed phases A and B.

Sb-rich cosalite

Cosalite is a common Bi- sulphosalt, ideally Pb

, with

several possible substitutions, including Ag, Cu, or Sb.

Recently Topa & Makovicky (2010) proposed the following

substitution mechanisms in cosalite: 1) Ag +Bi ↔ 2Pb at the

Me1 site; and 2) 2(Cu + Ag) ↔ Pb. They proposed these as

a result of the creation of vacancies in the Bi-containing octa-

hedral Me2 site accompanied by a progressive occupancy of

two triangular faces of this octahedron by Cu + Ag [i.e.,

Bi ↔ 2(Cu + Ag)]. This in turn is combined with the replace-

ment of Pb in the adjacent Me1 octa hedron by Bi. Their two

substitution mechanism combinations explain the closely fol-

lowed chemical relationship above.

Antimony for Bi substitution in cosalite is easier to explain.

Antimonian cosalite (up to Sb = 6.89 wt. %) was first described

by Lee at al. (1993) from the Dunjeon Au mine (Japan).

Cosalite with high Sb contents was also reported from Bacúch

(Pršek & Chovan 2001; Pršek 2008) and from Brezno-Hviezda

(Pršek et al. 2008) in the Low Tatras, Slovakia, with Sb

contents reaching values of up to 0.72 and 3.33 wt. %, respec-

tively. Sb-bearing cosalite with up to 4.33 wt. % of Sb was

also described by Cook (1997) from the Bi sulphosalt-

bearing, hydrothermal Pb–Zn mineralization at Baia Borşa,

Romania.

The cosalite from Stan Terg was previously described by

Terzić et al. (1974, 1975). He indicated, based on XRD and

EPMA results, that cosalite has up to 0.27 apfu Sb and up to

0.01 apfu Ag. The composition of cosalite measured by Terzić

falls between the results of the present study (Fig. 7). We

38.04

37.54

37.7

39.29

38.72

48.01

48.13

49.18

49.23

50.06

0.97

0.98

0.94

0.89

0.94

0.46

0.38

0.34

0.28

0.47

0.97

0.98

1.01

0.72

0.73

0.82

0.93

0.92

0.18

0.17

0.12

0.19

0.16

0.36

0.41

0.56

0.62

0.61

13.68

14.35

14.69

14.93

15.11

4.75

4.78

8.38

10.89

13.36

26.55

26.06

25.53

24.35

25.05

28.37

28.97

23.41

20.55

16.3

0.02

0.01

<MDL

0.02

<MDL

0.02

0.01

0.17

<MDL

0.01

<MDL

0.18

<MDL

0.05

<MDL

18.59

18.79

18.82

18.79

16.46

16.47

16.99

17.2

17.45

TOTAL

98.99

98.86

98.75

99.48

99.77

99.15

100.05

99.71

99.74

99.32

Chemical formula based on (Pb+Bi+Ag+Sb) = 26

Chemical formula based on (Pb+Bi+Ag+Sb) = 46

11.24

11.08

11.11

11.45

11.24

26.01

25.81

25.79

25.35

25.55

1.06

1.07

1.03

0.96

1.01

0.93

0.75

0.66

0.53

0.89

0.94

0.95

0.96

0.98

0.97

1.30

1.43

1.58

1.56

0.10

0.07

0.11

0.09

0.37

0.42

0.56

0.61

0.60

6.88

7.20

7.37

7.41

7.46

4.38

4.36

7.48

9.54

11.6

7.78

7.63

7.46

7.04

7.21

15.24

15.40

12.17

10.49

8.25

0.02

0.01

–

0.04

–

0.05

0.01

0.32

–

0.00

–

0.16

–

0.05

–

35.49

35.84

35.79

35.44

35.25

57.64

57.07

57.55

57.23

57.56

2.11

2.06

2.05

2.19

2.11

3.97

4.14

4.04

4.07

0.47

0.48

0.50

0.49

0.58

0.63

0.68

0.75

0.63

Notes: <MDL = below the minimum detection limit, Se was below the minimum detection limit in all analyses

Table 5: Representative EPMA analyses and atomic proportions for kobellite homologous series

minerals from sulphotelluride association: kobellite-tintinaite (1–5), izoklakeite-giessenite (6–10) in

the Stan Terg deposit.

377

Bi-SULFOTELLURIDES AND SULFOSALTS FROM THE STAN TERG DEPOSIT, KOSOVO

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, 2017, 68, 4, 366 – 381

suggest that the chemical composition of Stan Terg cosalite is

more complex than previously thought and depends on the

Ag + Cu and Bi + Sb contents. The cosalite composition from

Stan Terg is compared in Figure 10 to other Sb-rich cosalites

from diffe rent localities. The antimony content in the Stan

Terg cosalites is relatively high, but Cu+Ag substitution is rel-

atively limited.

Bi-rich jamesonite

Bi-rich jamesonite with significant high Bi content was

described from several hydrothermal vein occurrences in

Eastern Europe: Pršek et al. (2008) described jamesonite with

up to 2.41 apfu Bi, occurring with kobellite, eclarite and sul-

phosalts of the bismuthinite-aikinite group, from Brezno-

Hviezda, Slovakia. In the Úhorná locality (Slovakia) the Bi

content in jamesonite reaches 1.25 apfu, and this mineral was

found in association with tetradymite group minerals, tinti-

naite, and bournonite (Pršek & Peterec 2008). Pršek (2004)

reported from the Slovak Ore Mountains up to 1.20 apfu Bi in

jamesonite, hosted in siderite veinlets and associated with

kobellite homologues, jaskólskite, and Bi-bournonite.

Substitution of Bi for Sb is common in jamesonite from all the

above localities, which could suggest possible solid solution

Sb (at %)

Bi (at %)

Cu (at %)

Pb (at %)

Sb (at %)

Fe (at %)

Cu (at %)

Ag (at %)

Pb (at %)

izoklakeite-giessenite series

kobellite-tintinaite series
data from Kołodziejczyk et al.2015

1.2

1.4

1.6

1.8

1.2

1.4

1.6

1.8

0.2

0.4

0.6

0.8

0.2

0.4

0.6

0.8

Fig. 8. Binary plots showing chemical composition of kobellite homologous series from the sulphotelluride associa tion at the Stan Terg deposit.

A — Bi vs Sb at. %, B — Fe vs Cu at. %, C — Pb vs Ag at. %, D — Sb vs Cu at. %, E — Sb vs Ag at. %, F — Sb vs Pb at. %.

378

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GEOLOGICA CARPATHICA

, 2017, 68, 4, 366 – 381

with sakharovaite. Sakharovaite (ideally

FePb

(Sb, Bi)

) is considered to be

either a Bi-rich variety of jamesonite, or

a separate species, with Bi ↔ Sb substitu-

tion close to 50 at. % limit (Moëlo et al.

2008).

Similar sulphotellurides in hydro thermal

systems elsewhere

The sulphotelluride assemblages des-

cribed from the Stan Terg deposit com-

prise various phases accompanying

Bi-sulphosalts with low Ag contents. In

addition, neither native gold nor other

Au-bearing phases (e.g. Au-tellurides)

were identified in the paragenesis, thus

indicating that the sulphotellurides studied

may have precipitated from a hydrother-

mal fluid that was depleted in precious

metals. This is in contrast to the majority

of Bi-sulphotelluride enriched mineral

systems described in the literature, which usually host signifi-

cant Au and/or Ag contents.

Numerous Au–Ag–Bi–Te–S-bearing mineral systems have

been described elsewhere, and they are commonly interpreted

to have precipitated under either high-temperature hydro-

thermal (e.g., Czamanske & Hall 1975; Ren 1986), or

under epithermal conditions (e.g., Oberthür & Weiser

2008). Various phases from the tetradymite group minerals

(with unknown phases) together with sulphosalts were

described from plenty of localities worldwide (Gu et al.

2001; Cook & Ciobanu 2004; Pieczka et al. 2009;

Ciobanu at al. 2010; Cockerton & Tomkins 2012; Voudouris

et al. 2013).

Conditions of formation of the Bi–Pb–Sb–S–Te association

The Bi–Pb–Sb–S–Te mineral associations, found in the

external host rocks adjacent to the skarn-related orebody, are

closely related to previously described skarn-related and

breccia-filled types of mineral associations and reveal a simi-

lar high-temperature character of formation (Kołodziejczyk et

al. 2016 a,b). The sulphotelluride mineralization predates Ag

mineralization that formed in later stages of ore precipitation

at the Stan Terg deposit (Kołodziejczyk et al. 2016 a,b).

The sulphotelluride association in the Stan Terg deposit

seems to be closely related to cosalite and lillianite, and occurs

in most cases with ikunolite and native bismuth as inclusions

or as intergrowths with cosalite. The sulphotellurides could

have precipitated after galena as a result of introduction of Bi,

Sb and Te into the system by hydrothermal fluids, which

enabled the formation of Bi-sulphosalts and sulphotellurides.

The lamellar exsolution textures observed in lillianite at

Stan Terg, are similar to those described for the Ocna de Fier

Fe–Cu skarn deposit, Banat (southwest Romania) by Ciobanu

and Cook (2000), and indicate breakdown from the decom-

position of high-temperature initially formed crystals. The

temperature of initial mineralization may exceed 400 ºC as

suggested by Ciobanu & Cook (2000), in accordance with

experimental studies in the Cu–Pb–Bi–Ag-bearing systems

(Chang et al. 1988). As suggested by Ciobanu & Cook (2000)

for the Ocna de Fier, it is believed that intergrowths of

Bi-sulphosalts and sulphotellurides at Stan Terg reflect modu-

lated growth processes in a metasomatic environment.

Conclusions

A new occurrence of Bi-sulphotellurides at the Stan Terg

hydrothermal system, is associated with galena and Bi- and

Sb-sulphosalts.

The Bi-sulphotellurides include joséite-A, joséite-B, and

two other phases (phase A and phase B), that could not be

assigned to any known mineral due to the lack of structural

data. Bi ↔ Te substitution and admixtrure with submicro scopic

PbS and or Bi–Pb sulphotelluride layers, as well as lattice-scale

incorporation of Bi–(Pb)-rich modules are considered to

explain dispersion of our results along distinct geochemical

trends.

Cosalite from the Stan Terg deposit displays high Sb (max.

3.94 apfu), and low Cu and Ag (max. 0.72 Cu+Ag apfu)

contents.

Neither the sulphotellurides, nor the accompanying sulpho-

salts, incorporate abundant Ag in their structures. Gold and

silver sulphotellurides have not been found in this association.

The hydrothermal fluids could have been either depleted in

precious metals, or the physico-chemical conditions of ore

formation prevented Au and Ag precipitation at the site of ore

deposition.

38.71

38.81

38.58

38.33

37.58

37.81

36.91

37.07

2.51

2.66

2.79

2.94

2.39

2.36

2.48

2.22

0.01

<MDL

0.05

0.03

0.02

0.04

<MDL

0.01

28.75

26.77

26.06

25.39

22.24

21.78

20.41

19.57

8.15

10.94

11.11

13.16

16.21

17.66

20.24

21.05

<MDL

0.24

0.41

0.22

0.05

0.13

0.11

0.07

20.28

20.25

19.98

20.48

20.45

19.72

19.97

19.41

TOTAL

98.41

99.67

98.93

100.52

98.97

99.49

100.14

99.44

Chemical formula based on heavy metals = 11

4.05

4.03

4.01

3.97

4.11

4.09

4.01

4.09

0.98

1.02

1.08

1.13

0.97

0.95

1.00

0.91

0.00

–

0.02

0.01

0.02

–

0.00

5.12

4.73

4.61

4.47

4.14

4.01

3.77

3.67

0.85

1.13

1.15

1.35

1.76

1.90

2.18

2.30

0.00

0.09

0.16

0.08

0.02

0.05

0.04

0.03

13.73

13.58

13.42

13.69

14.45

13.79

14.01

13.83

Notes: <MDL = below the minimum detection limit, Se and Te were below the minimum detection limit in all

analyses

Table 6: Representative EPMA analyses and atomic proportions for representative Bi-rich

jamesonite from the Stan Terg deposit (wt. %).

379

Bi-SULFOTELLURIDES AND SULFOSALTS FROM THE STAN TERG DEPOSIT, KOSOVO

GEOLOGICA CARPATHICA

, 2017, 68, 4, 366 – 381

Pb+Bi+Sb

S+Se

bismuthinite

telluronevskite

Bi S

Bi TeS

Bi Te

(Pb,Bi) Te S

2.5

1.5

(Pb,Bi) Te S

saddlebackite

tetradymite

tsumoite

pilsenite

rucklidgeite

tellurobismutite

sulphotsumoite

joseite-B

joseite-A

baksanite

ingodite

Protojoseite line

ikunolite

Fig. 9. Ternary plot Bi+Pb+Sb vs S+Se vs Te of Bi-sulphotelluride minerals from the Stan Terg mine. Open circles: minerals ideal end member

chemical compositions; solid black symbols: chemical compositions of minerals from the Stan Terg deposit. Protojoseite line is drawn accord-

ing to general formula Bi

(Te,S)

given by Cook et al. (2007a).

Pb+Bi+Sb

S+Se

bismuthinite

telluronevskite

Bi S

Bi TeS

Bi Te

(Pb,Bi) Te S

2.5

1.5

(Pb,Bi) Te S

saddlebackite

tetradymite

tsumoite

pilsenite

rucklidgeite

tellurobismutite

sulphotsumoite

joseite-B

joseite-A

baksanite

ingodite

trend line

ikunolite

trend line

380

KOŁODZIEJCZYK, PRŠEK, VOUDOURIS and MELFOS

GEOLOGICA CARPATHICA

, 2017, 68, 4, 366 – 381

Fig. 10. Ternary plot Cu+Ag vs Bi+Sb vs Pb+Mn+Fe of cosalite — new EPMA data for Stan Terg, described as cosalite in the Stan Terg mine

and other Sb-rich cosalite.

Acknowledgements: The research was financed by the AGH

University of Science and Technology grants No. 11.11.140.320

and

15.11.140.636. Two anonymous reviewers are greately

acknowledged for their constructive comments that highly

improved the earlier version of the manuscript. Associate

Editor is especially thanked for the editorial handling of the

manuscript.

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