GeolCarp_Vol48_No6_387

GEOLOGICA CARPATHICA, 48, 6, BRATISLAVA, DECEMBER 1997

387–399

NEW DATA ON “PLUMOSITE” AND OTHER SULPHOSALT MINERALS

FROM THE HERJA HYDROTHERMAL VEIN DEPOSIT,

BAIA MARE DISTRICT, RUMANIA

NIGEL J. COOK

and GHEORGHE S. DAMIAN

Mineralogical Institute, University of Würzburg, Am Hubland, 97074 Würzburg, Germany

Department of Geology, Universtity of Baia Mare, 4800 Baia Mare, Rumania

(Manuscript received December 12, 1996; accepted in revised form October 15, 1997)

Abstract:

Compositional data on a range of sulphide and sulphosalt minerals from the hydrothermal vein deposit of

Herja in the Baia Mare metallogenic area are presented. The presence of zinkenite, chalcostibite, diaphorite, fülöppite,
boulangerite, bournonite, electrum and manganite are confirmed in the Herja ores for the first time. In addition,
compositions close to veenite, twinnite and heteromorphite have been identified — possibly representing the first
report of these minerals on Rumanian territory. Fibrous Sb-sulphosalts, which are trace phases in massive polymetallic
ores and are the main component of the abundant vugs and cavities, are dominantly jamesonite, although boulangerite,
berthierite and zinkenite are also present in lesser amounts. Arsenopyrite associated with the Sb-sulphosalts is com-
monly enriched in Sb (to 6 wt. %). Fahlore phases were determined to be tetrahedrite, with Ag contents ranging from
7 to 20 wt. %. All Sb-sulphosalts are free of As. The loose felty matted masses of acicular needles, „plumosite“, which
occur widely throughout the vein systems are confirmed to be jamesonite. This mineral is characterized by a con-
spicuous Mn content, equivalent to 4–8 % mol. % benavidesite. This has been partially confirmed by X-ray diffrac-
tion patterns, which showed a slight shift from those of some reference patterns for (Mn-free) jamesonite. However, a
quantitative correlation between cell parameters and extent of Mn substitution is prohibited by discrepancies in the
various peak patterns, resulting from differing experimental conditions. Although „plumosite“ has been regarded as
synonymous with boulangerite in recent years, it is proposed that the descriptive name „plumosite“ be used for all such
felted masses of Pb-Sb sulphosalts, including those with the compositions of jamesonite and berthierite. No supportive
evidence for the existence of the problematic mineral parajamesonite was found in the examined samples. Geothermo-
metry based on the S-isotope compositions of coexisting pyrite-galena pairs indicated temperatures of 417 ± 75

C and

320 ± 70

C, which are regarded as close to the maximum temperatures at the onset of mineralization. The stibnite and

sulphosalt parageneses, however, are believed to have formed at temperatures below 220

Key words:

Rumania, Herja, hydrothermal vein mineralization, Pb-Sb sulphosalts, jamesonite, plumosite.

Introduction

The Herja deposit, formerly known by the Hungarian names
Kisbánya and Herzsabánya, has been mined since medieval
times. It is one of the largest of the hydrothermal vein sys-
tems of Pannonian age hosted within Samartian-Pannonian
volcanic rocks and Neogene and Paleogene sediments in the
metallogenic district surrounding the city of Baia Mare in
Maramure County, northern Rumania. The polymetallic
mineralized veins at Herja contain a wide variety of Pb-Sb
sulphosalts and Herja is the type locality for fizelyite
(Pb

) as well as the poorly constrained para-

jamesonite (FePb

Despite the mineralogical complexity and the notoreity of

beautiful and spectacular museum specimens (c.f. Huber &
Mure an 1996), the mineralogy of the Herja ores has not
been studied in detail using modern microanalytical methods
and compositional data on component phases are largely
lacking. Although this preliminary study on a limited number
of samples cannot in any way claim to be representative of
the entire vein system, it represents a first contribution to the

study of mineral compositions within the Herja deposit and
serves as a basis for future work.

In this short paper, our aim is firstly to report compositional

data on a number of sulphide and sulphosalt phases from Her-
ja, in many cases for the first time. Our preliminary study is
based on investigation of massive Pb-Zn rich ores and the
cavity fillings containing stibnite and other Sb-bearing miner-
als. Eight further Pb-sulphosalt minerals not previously re-
ported from Herja (zinkenite, fülöppite, boulangerite, bourno-
nite, heteromorphite, veenite, diaphorite, twinnite) have been
found in samples from recently opened parts of the mine.
These are also described and compositional data presented.
Veenite, heteromorphite and twinnite have not been previous-
ly reported on Rumanian territory. Chalcostibite is also de-
scribed from Herja for the first time, although its presence was
mentioned by Uduba a et al. (1992). Secondly, new data on
the abundant „plumosite“ at Herja is presented, with a sug-
gested redefinition of this term. The existence of both jameso-
nite and its dimorph parajamesonite at Herja is discussed in
the light of new data. In addition, new estimates for the tem-
perature of crystallization are available, based on the S-isotope
composition of sulphide pairs from the Herja ores.

388 COOK

and DAMIAN

Geological setting of the mineralization

The deposit, situated in the Gutâi Mts., about 6 km NE of Baia

Mare consists of two major groups of veins along ENE-WSW
oriented fractures related to a subvolcanic body of pyroxene
andesite and porphyritic quartz microdiorite (Figs. 1–2). The
southern vein group, including the veins âlan (also known
as vein 10), Zincos (vein 20), Igna iu (vein 40), Clementina
(vein 60), Boromei (vein 80), and Mächtige (vein 100), which
were the source of historic production, are enclosed by the
porphyritic quartz microdiorite body. The northern vein group
(numbered 30, 50, 70, ... up to 170) lies within altered sedi-
mentary rocks of Pannonian, Sarmatian and Eocene age. De-
scriptions of host rock geology, structural controls and hydro-
thermal alteration have been given by Petrulian (1934), Szöke
(1968), Borco & Lang (1973), Borco et al. (1975) and Lang
(1979). A comprehensive account of geology, petrology,
geochemistry and mineralogy has recently been presented by
Damian (1996). Age constraints have recently become available
(Edelstein et al. 1992; Lang et al. 1994); andesitic volcanism in
the Gutâi Mountains extended between 13.4 and 9.0 Ma. Hy-
drothermal activity in the area took place between 11.5 and
8.0 Ma; the Herja mineralization having been dated by Edel-
stein et al. (1992) using K-Ar methods on illite at 8.8 ± 0.6 Ma.

Borco et al. (1975) described the main veins in the southern

part of the Herja deposit in some detail. Unlike other deposits
in the Baia Mare metallogenic area (e.g. Cavnic, Baia Sprie),
there is little evidence of vertical zonation within the vein sys-
tem, with Pb and Zn being rather evenly distributed over the
depth of the system, which probably exceeds 1000 m and a
width of more than 1200 m. A total of more than 180 veins
have been identified to date. The polymetallic ores are charac-
terized by the geochemical signature Zn > Pb ± Cu, Ag, Au,
with significant enrichment in Sb, As, Cd, Bi, Ga, In, Mn, W
and Tl. Borco et al. (1975) recognized a single phase of min-
eralization, beginning with the deposition of pyrite and pyr-
rhotite and followed by intense crystallization of sphalerite
and galena, followed in turn by stibnite and various sulphos-
alts at lower temperatures. Idiomorphic chalcopyrite, galena,
marcasite and quartz were deposited later in the sequence.
Temperatures of mineralization were previously estimated to
be in the range 250–350

C on the basis of fluid inclusion data

(e.g. Pomârleanu 1971). Vein thickness may attain dimensions
as large as 2 m, but are significantly lower in the many minor
vein branches, where thicknesses of only 1–2 cm are common.

Alongside massive ore composed of sphalerite, galena and

subordinate chalcopyrite, with pyrite, pyrrhotite and marca-
site, in which Ag-bearing tetrahedrite and other sulphosalts
are minor components, the mineralization also contains abun-
dant vugs and mineralized cavities in which a large variety of
Pb-Sb sulphosalt phases are well developed. The Herja mine
is particularly famous for centimeter-sized tetrahedrite, nee-
dle-like jamesonite, berthierite and stibnite, semseyite and the
abundant felted masses of „plumosite“ (Federerz). The vug as-
sociations are accompanied by quartz, spheroidal black and
white calcite and also siderite. The sulphosalt and stibnite-
containing vugs were particularly abundant at upper levels
which are now largely mined out. Antimony was the most im-
portant product of mining prior to 1928. Other ore minerals re-

ported include arsenopyrite, mackinawite, bournonite, molyb-
denite, pyrargyrite, argentite, fülöppite, gold and electrum.
Dolomite, rhodochrosite, flourite, gypsum and vivianite are
accessory gangue phases.

Our sample suite is drawn from both the northern and

southern vein groups. Massive ores varied petrographically
from massive galena, galena-chalcopyrite and galena-
sphalerite varieties, with or without pyrite, to marcasite- and
pyrrhotite-rich types. Other samples contained only quartz
with minor sulphides. Samples with coarse stibnite, jameso-
nite and berthierite crystals were collected from cavities as
were felty masses of „plumosite“.

Analytical methods

All electron probe microanalyses were carried out on the

CAMECA SX-50 instrument in Würzburg. Standards and radia-
tions used were as follows: pure Bi (M

), pure PbS (Pb-M

AsGa (As-L

), FeS

(Fe-K

, S-K

), pure Cu (K

), ZnS (Zn-

), pure Ni (K

), pure Co (K

), pure Te (L

), pure Se (L

pure Ag (L

), pure Au (M

), HgS (Hg-M

), Sb

(Sb-L

MnTi (Mn-K

). No other elements were detected in any of the

minerals analysed. A beam current of 15 nA and an accelerating
voltage of 15 kV were used. All mineral grains and standards
were analysed under the same operating conditions. Minimum
detection limits are ca. 0.1 wt. % for all elements. At least one
analysis was carried out on each grain. Tables 1 to 5 contain anal-
yses representative of the total data suite.

Determination of sulphur isotope concentrations was made

on 9 sulphide separates which are considered to be representa-
tive. The coarse grain size and high degree of purity permitted
the separation by hand-picking of grains. All S-isotope analy-
ses were carried out on a Finnegan MAT-251 gas spectrometer
at the Institut für Geochemie, Universität Göttingen. Analyti-
cal errors are approximately 0.1–0.2 ‰

The X-ray diffraction data obtained on “plumosite” was ob-

tained on a Philips PW 1710 diffractometer with secondary
graphite monochromator. Filtered Cu K

1,2

radiation was used;

= 1.5418 A. Instrumental conditions were 40 KV and 30 mA.

Measurement was carried out between 2

values of 4–80

, in

steps of 0.02

and a counting time of 5 secs at each step. The

sample material was held in a single crystal quartz plate. 407 re-
flections were recorded (within the interval 9.55 < d > 1.87).
Peak positions and intensities were indexed by the diffractome-
ter computation program. Our methods are thus comparable to
those used to obtain diffraction spectra for jamesonite (Berry
1940; Garavelli 1958) with which the diffraction data for „plu-
mosite“ will be compared in this paper, although complete ana-
lytical details are not given for these earlier patterns. In contrast,
the reference pattern for benavidesite (Oudin et al. 1982) was
obtained by powder film methods.

Sulphide mineral compositions

Sphalerite

Two compositional varieties of sphalerite were recognised

(Table 1, columns 1–3). The earlier, and more abundant vari-

392 COOK

and DAMIAN

ety is characterized by a deep red colour and high Fe content
(mean FeS contents > 18 mol. %), accompanied by enrich-
ment in Mn (0.2–0.5 wt. %). Concentrations of Cd are vari-
able but relatively low. The second, darker, type accompa-
nies the late sulphosalt parageneses and has a mean Fe
content of only 3.2 mol. % FeS and no detectable Mn. This
type is further characterized by an enrichment in Cd (mean
0.33 wt. %). Enrichment in Cd in a late sphalerite can be re-
lated to the strong incompatibility of that element in the lat-
est generation of hydrothermal fluids.

Galena

Analyses of galena (Table 1, columns 4, 5) from the total

sample suite showed little variation between textural types. In
all samples, trace amounts of Ag, Bi, Sb and, occasionally, Se
were detected. Typical contents (all in wt. %) are 0.15–0.45
for Bi, 0.10–0.24 for Ag, 0.12–0.28 Sb and < 0.10–0.13 Se.

Arsenopyrite

Arsenopyrite was observed in all of the sulphosalt-rich

samples, but was absent in massive ores. It is an extremely
abundant phase in the sulphosalt-rich suite, occurring as
small euhedra in association with jamesonite, boulangerite,
berthierite, tetrahedrite or semseyite in a sphalerite-galena
matrix, or as larger grains, commonly overgrown by fibrous
sulphosalts (Fig. 3a). Compositions are uniformly close to
Fe

1.00

(As,Sb)

0.90

1.05

(Table 1, columns 6, 7). Considerable

localised enrichment in Sb was however noted in a number
of samples, up to as much as 6.65 wt. % in some analysed
grains, which corresponds to 10.1 % end member gudmun-
dite. Some grains showed evidence of zonation in which the
cores were richer in Sb (to 6 wt. %) than the rims (< 1 wt. %
Sb). This pattern could not, however, be verified in all grains

on which microanalytical profiles were made. In some cases,
there appeared to be no zonation, and in others a rather errat-
ic pattern was evident, possibly related to repeated crystalli-
zation and resorption during deposition.

Pyrite and marcasite

In the single sample in which it was analysed, pyrite was

found to contain minor quantities of As to 0.12 wt. %. Marca-
site (Table 1, column 8), which was formed relatively late in
the paragenetic sequence was found, in contrast, to contain de-
tectable Sb in almost all cases, at concentrations typically of
0.10 to 0.30 wt. %, but as much as 2.1 wt. % in isolated cases.

Bournonite

Analysed bournonite compositions (Table 2, column 1) were

stoichiometric CuPbSbS

. Very limited solid solution towards

the As end-member, seligmannite and only minor trace Bi and
Te were noted.

Tetrahedrite-tennantite

Tetrahedrite is abundant in the Herja ores and is probably the

most important Ag-carrier in the vein ores. Tetrahedrite is
present as euhedral crystals, ranging from 20 µm to several
mm in size and commonly contains inclusions of other sulpho-
salts (Fig. 3b). Microprobe analyses (Table 2, columns 2–5) in-
dicate that Ag-rich tetrahedrites (16–20 wt. % Ag) prevail in
the samples studied, although there is a marked inverse corre-
lation between Ag content and grain size, the largest grains
(> 2 mm) containing less than 10 wt. % Ag. Contents of As are
negligible (< 0.20 wt. %) and atomic Fe/Zn ratios generally ex-
ceed 5. The formulae of tetrahedrite from all the representative
analyses given in the table give a slight excess of both Sb and S
over expected stoichiometry, when calculated to 12 metal at-

Sphalerite (8255; GV-100, HJ-13)

Galena (8255, HJ-12)

Arsenopyrite (4, HJ-12)

Marcasite (HJ-11)

mean

n=2

n=3

n=2

n=5

n=12

n=8

n=11

n=5

0.13±0.01

11.54 ±0.11

1.78 ±0.35

8.66 ±0.29

35.10±0.65*

34.69 ±0.83

45.66 ±0.52

53.95 ±0.19

62.78 ±0.46

55.82 ±0.32

0.46 ±0.02

0.24 ±0.02

0.11 ±0.01

0.33 ±0.02

0.28 ±0.01

0.12 ±0.07

0.19 ±0.06

86.84 ±1.00 86.80 ±0.63

0.16 ±0.07

0.28 ±0.08

1.68 ±1.08

4.90 ±2.22

1.11 ±0.79

41.38 ±1.68 38.36 ±2.49

0.03 ±0.07

0.33 ±0.10

0.27 ±0.11

32.59 ±0.34

32.98 ±0.20

33.58 ±0.44 13.27 ±0.12 13.71 ±0.17 21.22 ±0.79 21.80 ±0.54

52.04 ±0.70

0.10 ±0.06

0.14 ±0.10

0.03 ±0.05

Total

98.65

98.00

98.58

100.82

101.28

99.38

99.89

98.84

Formulae:

(Zn

0.80

0.20

(Cd,Mn)

0.01

)

1.01

0.99

(Zn

0.97

0.03

(Cd,Mn)

0.01

)

1.01

1.00

(Zn

0.83

0.15

(Cd,Mn)

0.01

)

0.99

1.00

(Pb

1.01

(Bi,Ag,Sb)

0.01

)

1.02

1.00

(Pb

0.98

(Bi,Ag,Sb)

0.01

)

0.99

1.00

(As

0.88

0.02

)

0.90

1.05

* including 0.04 % Co

1.00

(As

0.83

0.06

)

0.89

1.10

(Fe

1.00

(As,Sb)

0.01

)

1.01

0.99

Table 1:

Electron probe microanalyses of sulphides.

NEW DATA ON “PLUMOSITE” AND OTHER SULPHOSALT MINERALS 393

oms; ranging between (Ag

1.17

8.78

1.49

0.55

)

(Sb

4.20

As,Bi

0.01

)

4.21

13.26

and (Ag

3.62

6.58

1.60

0.20

)

4.22

13.60

Higher Ag/(Ag+Cu) ratios tend to correlate positively with higher
Fe/(Fe+Zn) ratios in the sample suite, with a dramatic rise in
Ag content over the Fe/(Fe+Zn) range 0.7 to 1.0 (Fig. 4).

Although the problem was not experienced among the Ag-

poorer varieties, some of the tetrahedrites richest in Ag gave
poor totals. This, and the fact that (Fe+Zn) are consistently
less than 2.00 atoms p.f.u. in many of these analyses, urges
considerable caution in their interpretation; an excess in
(Cu+Ag) beyond 10 atoms p.f.u. has been reported to be rou-
tinely not detected by electron microanalysis (Lind & Mak-
ovicky 1982). The choice of microprobe standards used,
which did not include synthetic sulphosalt standards, may
also infer that some caution be exercised in the interpretation
of analytical data.

Semseyite

Semseyite is relatively abundant in the investigated sam-

ples, as coarse grains, commonly associated with tetrahedrite,
galena or sphalerite and infilling cavities. Compositional vari-
ation would appear to be extremely limited in semseyite,
Pb

(Table 2, columns 6–8). We note, however, minor

contents of Ag, Cu and Bi in some analyses, one sample con-
taining a particularly Ag-enriched variety. Furthermore, there
is minor variation in the Pb/Sb ratio, with some samples
showing a consistent slight deficiency in Pb below 9 atoms
p.f.u. and a corresponding enrichment in Sb (Table 2, column 6)
and the opposite situation in other samples. Although a sys-
tematic analytical error cannot be ruled out, this is considered
unlikely as the analyses were accumulated at different times,
using different calibrations and operating conditions. Further-
more, other Pb-Sb sulphosalts analysed at the same time gave
stoichiometric formulae. The data rather suggest that there
may be intergrowths of more than a single Pb-Sb-S phase
present, at the microscopic or sub-microscopic scale, thus re-
sulting in nonstoichiometric compositions.

Fülöppite

Fülöppite, which occurs as short prismatic crystals, within

a gangue matrix or intergrown with sphalerite, galena,
zinkenite and stibnite is essentially stoichiometric in com-
position (Pb

), except for very minor Ag, Bi and Te

(Table 2, column 9).

Berthierite

Berthierite occurs as acicular grains, very similar in appear-

ance to jamesonite. These occur either in gangue matrix or in-
tergrown with the antimonian arsenopyrite. Electron probe mi-
croanalysis of berthierite, FeSb

indicates the incorporation

of significant amounts of Mn (0.25–0.5 wt. %) in the structure,

Table 2:

Electron probe microanalyses of sulphosalt minerals.

Bournonite

(8255)

Tetrahedrite (110, 50D, HJ-13, HJ-14)

Semseyite (4, GV-10, SI-480)

Fülöppite

(GV-100)

√

≈

∆

mean

n=5

n=1

n=17

n=5

n=9

n=6

n=9

13.08+0.31

25.57±0.09

22.09

31.71±1.20

22.97±0.41

5.15±0.09

5.12

4.74±0.87

5.47±0.12

0.85±0.15

0.65

2.06±1.01

0.86±0.04

0.03±0.05

15.77±0.41

21.21

7.17±1.56

19.57±0.23

1.24±1.54

0.10±0.05

0.09±0.12

42.01±0.38

52.31±0.90

52.55±2.36

51.62±0.74

29.29±0.34

25.07±0.13

27.03±0.22

27.06

29.07±0.28

27.37+0.21

28.32±0.36

27.26±0.64

27.41±0.37

47.50±0.61

0.17±0.04

0.12±0.02

0.02±0.01

0.01±0.01

0.09±0.09

0.10±0.04

0.26

0.10±0.07

0.12±0.07

0.23±0.05

0.18±0.07

0.20±0.07

0.07±0.09

9.42±0.13

23.43±0.27

22.84

24.25±0.23

22.61±0.19

19.08±0.16

18.67±0.35

19.18±0.24

23.09±0.21

0.03±0.04

0.11±0.05

0.16

0.10±0.04

Total

99.87

98.03

99.23

99.01

98.97

99.94

99.92

98.61

100.08

Formulae:
¿

1.02

1.00

(Sb

1.02

0.01

)

1.03

≈ Pb

8.91

(Sb

8.21

0.04

)

8.25

(Cu

7.39

1.69

0.24

2.68

)

12.00

(Sb

4.07

0.03

0.01

)

4.11

13.42

∆ (Ag

0.42

9.14

)

9.56

(Sb

8.07

0.03

)

8.10

20.99

0.01

)

(Cu

6.46

1.70

0.18

3.65

)

12.00

(Sb

4.13

0.02

)

4.15

13.24

0.02

)

13.26

« (Ag

0.03

8.78

)

8.81

(Sb

7.91

0.03

)

7.94

20.97

0.03

)

√

(Cu

8.78

1.49

0.55

1.17

)

12.00

(Sb

4.20

0.01

)

4.21

13.26

»(Zn

0.01

0.02

2.94

)

2.98

(Sb

8.13

0.01

)

8.14

(Cu

6.63

1.80

0.24

3.33

)

12.00

(Sb

4.13

0.01

)

4.14

12.95

Fig. 4.

Plot of Fe/(Fe+Zn) against Ag/(Ag+Cu) for analysed tetra-

hedites, indicating silver enrichment in Zn-poor varieties.

394 COOK

and DAMIAN

together with minor Cu, Zn, Ag, Pb, As and Bi at trace levels in
a portion of the analyses (Table 3, columns 1, 2).

Zinkenite

Zinkenite is an abundant mineral in the investigated sam-

ples, occurring embedded in sphalerite as elongate fibrous
grains up to 1.0 mm in length, either as dense often radial ag-
gregates (Fig. 3c) or as isolated blades. Compositional varia-
tion would appear to be extremely limited, without detect-
able Cu and close to ideal stoichiometry (Pb

), except

for minor Ag and Bi (Table 3, column 3).

Boulangerite

Boulangerite (Pb

) is a widespread component,

both as fine-grained aggregates and as blunt needles, associ-
ated with tetrahedrite, sphalerite and galena (Fig. 3d). Bou-
langerite was not seen in intimate association with zinkenite
or jamesonite. Compositionally, the mineral is close to sto-
ichiometric (Table 3, column 4). Some analyses of the nee-
dle-shaped grains did, however, show a deficiency in Pb and
enrichment in Sb, towards the composition Pb

4.65

4.35

Boulangerite has been shown to show significant variation in
composition (Mozgova et al. 1983). These authors intro-
duced the name plumosite for Pb-poor compositions compa-
rable to those described here and falkmannite for Pb-rich,
Sb-poor varieties. Plumosite sensu Mozgova et al. (1983)
did not receive acceptance as a distinct mineral phase, and
should be regarded as Pb-poor boulangerite. Furthermore,
this should not be confused with the Herja „plumosite“ dis-
cussed in a later section of this paper.

Heteromorphite (?)

Compositions of a Pb-Sb-S phase, concordant with that of

the mineral heteromorphite (Pb

) are reported from the

Baia Mare area for the first time. The phase occurs as small
elongate grains, intimitely intergrown with zinkenite en-
closed in a sphalerite matrix. Microprobe analyses indicate

close to ideal stoichiometry (Table 3, columns 5, 6). The mi-
nor Zn detected in some analyses may best be attributed to
the surrounding sphalerite.

Veenite (?)

Similarly, compositions concordant with those of the min-

eral veenite (Pb

) are also reported for the first time

from the Herja deposit. Only seen in a single sample, grains
with this composition occur as a fine reaction rim, about
50 µm thick between galena and an aggregate of jamesonite.
Electron probe microananalysis (Table 3, column 7) indicat-
ed the composition to be stoichiometric.

Twinnite (?)

In the sample from the upper part of the Clementina vein

(GV-100) which also contains zinkenite, fülöppite and het-
eromorphite, a number of small grains were detected whose
composition closely matches that of the rather rare sulphosalt
twinnite, PbSb

, (Jambor 1967; Bracci et al. 1980). Similar

in appearance and composition to the twinnite described by
Moëlo et al. (1983), our grains contains no As. With the ex-
ception of minor Ag and Bi (Table 4), the analysed composi-
tions fit very closely to the stoichiometry of twinnite. How-
ever, since twinnite has a dimorph, guettardite, only a
tentative identity may be assigned to the PbSb

phase in

the absence of supporting X-ray data. However, this repre-
sents the first reported occurrence of either of these rare min-
erals on Rumanian territory.

Diaphorite

Electron probe microanalyses of diaphorite are summa-

rized in Table 4. Although generally stoichiometric with re-
spect to (Ag+Pb):Sb:S ratios, the Herja diaphorite is charac-
terized by a conspicuously high Ag/Pb ratio, which exceeds
1.5 in all analyses. Although the number of chemical or
microprobe analyses of diaphorite reported in the literature is
small (an overview was given by Hoffmann et al. 1977), con-

Table 3:

Electron probe microanalyses of sulphosalt minerals.

Berthierite

(H-210, HJ-11)

Zinkenite

(GV-100)

Boulangerite

(HJ-14)

Heterom orphite

(GV-100, HJ-12)

Veenite

(HJ-13)

√

≈

∆

mean

n=7

n=5

n=11

n=16

n=5

n=3

n=2

11.81±0.15

12.74±0.08

M n

0.25±0.04

0.26±0.05

0.04±0.02

0.02±0.02

0.25±0.12

0.04±0.03

0.02±0.03

0.16±0.05

0.10±0.12

0.03±0.05

0.15±0.17

2.02±0.64

31.70±0.44

54.31±0.55

46.87±0.56

47.69±0.90

50.35±0.03

56.17± 0.26

54.68±0.50

44.72±0.47

26.33±0.32

30.74±0.64

31.42±1.10

29.71±0.32

0.13±0.04

0.13±0.07

0.19±0.09

0.17±0.08

0.28±0.09

0.09±0.03

0.05±0.05

29.39±0.34

28.89±0.09

22.58±0.17

18.58±0.26

20.08±0.26

19.89±0.16

19.47±0.17

Total

97.92

98.76

99.35

99.51

98.25

99.13

99.58

Form ulae:

¿ (Fe

0.92

M n

0.02

(Cu,Ag,Pb)

0.01

)

0.95

2.01

(Zn

0.11

0.01

6.86

)

6.98

(Sb

7.66

0.04

)

7.70

¡ (Fe

1.01

M n

0.02

(Cu,Ag,Pb)

0.04

)

1.07

2.00

≈

(Zn

0.02

0.00

7.04

)

7.06

(Sb

7.90

0.01

)

7.91

¬ (Ag

0.09

9.12

)

9.21

(Sb

21.90

0.05

)

21.95

∆

2.01

√ (Ag

0.02

4.98

)

5.00

(Sb

4.10

0.0l

)

4.11

NEW DATA ON “PLUMOSITE” AND OTHER SULPHOSALT MINERALS 395

siderable variation in the Ag/Pb ratio would appear to be
characteristic. Mozgova et al. (1989) addressed composition-
al variation in diaphorite, citing microanalytical and crystal
structural data from various deposits. They argued that a
continuous solid solution series exists between diaphorite
(Ag

) and a phase with the formula Ag

PbSb

for which they proposed revival of the name „brongniardite“
(sic.). Mozgova et al. (1989) considered that this latter phase,
with Ag/Pb ratios between 1.75 and 2.00 may be considered
as an Ag-rich diaphorite. Our data would appear to strongly
support such an argument, in that the Herja diaphorite exhib-
its a wide range of Ag/Pb ratios, from 1.53 to 1.69. Further-
more, we note anomalously high Ag/Pb ratios in diaphorite re-
ported from other localities, e.g. the recently described diaphorite
from the Apuan Alps, Italy which has a Ag/Pb ratio of 1.67 (Friz-
zo & Simone 1995).

Chalcostibite

Also confirmed for the first time from Herja is chalcostib-

ite. This mineral is present as coarse blastic grains and nee-
dle-like crystals, associated with a range of other Sb-sulpho-
salts (Fig. 3e). Microanalysis of 9 grains gave a mean
formula of Cu

0.99

1.02

Jamesonite

Extremely abundant in all of the sulphosalt-rich samples,

jamesonite, Pb

(Fe>Mn)Sb

, occurs as fibrous crystals

up to 1 cm in length growing within gangue and overgrow-
ing earlier formed minerals, notably arsenopyrite and tet-
rahedrite (Figs. 3a–b). Less commonly, jamesonite also
occurs in thick dense aggregates, particularly as a reaction
rim between galena and tetrahedrite (Fig. 3f). The felted
„plumosite“ masses were also identified as being exclu-
sively jamesonite. Microanalysis of jamesonite from all
textural types revealed extensive homogeneity in composi-
tion (Table 5). Noteworthy is the consistent Mn content,
which ranges from 0.09 to a maximum of about 0.25 wt.
%, corresponding to about 4–8 mol. % of the ideal Fe-free

Mn-rich end-member bénavidésite. This is discussed fur-
ther, with reference to X-ray diffraction data, in a later sec-
tion. Almost all analysed jamesonite grains contained de-
tectable Ag and Bi. Particularly the coarse fibrous
„plumosite“ was found to be Ag-rich, commonly exceeding
0.20 wt. %.

Other minerals

Two small grains of electrum were observed (12 and 8 µm

in diameter). Both gave compositions close to Au

0.5

(65 wt. % Au, 35 wt. % Ag). The presence of Hg, Cu or other
metals was not detected. Stibnite (Sb

) is abundant. All mi-

croanalyses gave perfect stoichiometry — no other elements
were present. Manganite, Mn(OOH) was recognized; the mean
composition was determined to be (in wt. %) 0.30 SiO

, 0.08

MgO, 0.42 CaO, 78.38 MnO, 0.39 BaO, giving a calculated
formula of (Mn

0.98

0.01

(Mg,Si,Ba)

0.01

)

1.00

OOH, assuming

ideal stoichiometry.

„Plumosite“

Fibrous aggregates known as „plumosite“ are known from

many of the mines in the vicinity of Baia Mare and in other
Miocene vein type deposits elsewhere in northern Rumania
(Uduba a et al. 1993). These authors remarked upon the mor-
phology of these felt-like masses which may reach several cm
in width and thickness, and incorporate small (1–2 mm) sized
crystals of sphalerite, galena, tetrahedrite, quartz and siderite.
Earlier, Mo iu et al. (1972), Ghiurca & Mo iu, (1986) had de-
scribed plumosite from Herja (of jamesonite composition, like
in the present study) which, in some cases, forms as curved
crystals and concentric rings. Uduba a et al. (1993) note that
most „plumosite“ is of jamesonite composition, although bou-
langerite dominates in some deposits, and robinsonite in the
Săsar vein system.

The term „plumosite“ has been used to describe fibrous va-

rieties of a number of Pb-sulphosalts over the past 150 years

Table 4:

Electron probe microanalyses of twinnite and diaphorite.

Twinnite (GV-100)

Diaphorite (GV-10)

mean

max.

min.

mean

max.

min.

n=7

n=6

0.02±0.05

0.12

0.10±0.09

0.19

0.12±0.01

0.14

24.73±0.23

24.92

24.34

34.60±1.14

37.45

34.29

28.03±0.35

28.34

27.44

42.68±1.01

43.52

40.16

26.50±0.25

26.85

26.17

0.20±0.11

0.27

0.11±0.11

0.27

22.02±0.36

22.47

21.40

19.18±0.29

19.46

19.23

0.02±0.05

Total

99.62

98.69

Formulae:

(Ag

0.01

0.97

)

0.98

(Sb

2.04

0.01

)

2.05

(Cu

0.01

0.02

3.06

)

3.09

1.81

(Sb

2.91

0.01

)

2.92

396 COOK

and DAMIAN

but is presently considered as being synonymous with bou-
langerite, Pb

(Mumme 1989; Clark 1993). We would

suggest usage of the term plumosite in the sense of Chace
(1948) „as a descriptive term which may be applied to jame-
sonite, boulangerite, zinkenite, any other lead sulphosalt, or
as mixture thereof, that has a plumose texture or that occurs
in a fibrous aggregate“.

Usage of the name plumosite is further complicated fol-

lowing the proposal of Mozgova et al. (1983). On the basis
of analysis of compositional and structural investigations of
falkmanite and boulangerite, these authors suggested that the
name plumosite be revived for Pb-poor boulangerite
(Pb

<4.7

>4.2

). Falkmanite, boulangerite and „plumosite“

were proposed to belong to the „boulangerite homologous
series“, with the general formula Me

. According to these

authors, there is a compositional gap between boulangerite
and their „plumosite“ (see also discussion in Am. Mineral.,
69, 411). Mumme (1989) addressed the crystal structure of
near ideal composition boulangerite, and noted that there
are considerable difficulties related to a series of minerals
extending from falkmannite through boulangerite to plu-
mosite (sensu Mozgova et al. 1989). Furthermore, Mumme
(1989) noted the apparent structural identity of „plumosite“
(sensu Mozgova et al.) to jaskolskiite and suggested that this
mineral, with the composition Pb

4.8

4.2

to Pb

4.4

(general formula Pb

) analysed by Mozgova & Bortni-

kov (1980) and Mozgova et al. (1983), may in fact be a dis-
crete phase within the meneghinite homologous series.

X-ray diffraction

A previous X-ray diffraction study of „plumosite“ from

Herja (Uduba a 1992) showed the phase to correspond to
jamesonite, although a slight peak shift and divergence in the
unit cell parameters was noted when the diffraction pattern
was compared with literature data for jamesonite. Incorpora-

tion of Ag, Mn and Tl at concentrations of 6000, 400 and
250 ppm respectively, were reported in the investigated sam-
ple. It was concluded that the relatively high Mn content of
the Herja „plumosite“ causes this shift towards the Mn-ana-
logue of jamesonite, benavidesite, Pb

(Mn,Fe)Sb

(Oudin

et al. 1982; Chang et al. 1987).

Subsequently, Uduba a et al. (1993) showed, using a num-

ber of „plumosite“ samples from different occurrences in
northern Rumania, that the cell parameters can be positively
correlated with Mn content. It is not entirely clear which role,
if any, the substitution of Ag (which has been confirmed in the
present study) and Tl play in modification of unit cell dimen-
sions. These authors interpret „plumosite“ to have been one of
the latest minerals to have crystallized from hydrothermal so-
lution and argue, for this reason, that they have collected the
relatively incompatible elements Tl and Mn.

X-ray diffraction studies carried out in the present study

confirm the earlier results. Diffraction patterns for Herja
„plumosite“ from vein 90, level-5, together with those of
jamesonite (JCPDS-ICDD Card 13-461, after Garavelli
1958) and of benavidesite from Uchucchacua, Peru (Oudin et
al. 1982), which had a Mn/(Fe+Mn) ratio of 0.61, are given
in Table 6. Four other samples of „plumosite“ from Herja
gave identical X-ray diffraction spectra to that quoted in the
table. Comparison of the diffraction spectra with published
data for jamesonite (Berry 1940; Garavelli 1958) would ap-
pear to show a relatively strong shift in the positions of all
major peaks towards those of benavidesite, as determined by
Oudin et al. (1982). This is commensurate with the microan-
alytical data described above showing 4–8 mol. % of the Mn
end member present within the Herja „plumosite“. However,
the reader will note that there are considerable discrepancies
in the peak patterns between those given by Berry (1940) and
Garavelli (1958) for end-member jamesonite. These differ-
ences are sufficiently large that the shift in peak positions
cannot be readily correlated with Mn substitution. Indeed,
the peak positions for Herja „plumosite“ given in Table 6 are

Table 5:

Electron probe microanalyses of jamesonite.

G V -10

606b

H J-12

H J-13

H J-15

√

m ean

n=3

n=8

n=13

n=25

n=5

C u

2.28±0.15

2.49± 0.16

2.65±0.240

2.48± 0.11

2.47±0.06

M n

0.22±0.09

0.16± 0.07

0.09±0.04

0.11± 0.03

0.11±0.01

Z n

0.05±0.07

0.06± 0.15

0.04±0.06

A g

0.61±0.86

0.04± 0.07

0.20±0.05

0.01± 0.01

0.22±0.16

38.16±0.52

39.63 ±0.45

39.00±0.28

39.10± 0.45

38.54±0.84

34.47±0.27

34.43 ±0.34

35.91±0.41

35.36± 0.42

35.70±0.47

A s

B i

0.09±0.13

0.15± 0.13

0.15±0.11

0.30± 0.23

0.16±0.08

21.77±0.23

21.46 ±0.30

21.63±0.28

21.28± 0.22

21.50±0.19

T e

0.02±0.05

T otal

97.65

98.42

98.67

98.63

98.70

F orm u lae:

¿ (Fe

0.84

0.02

M n

0.08

)

0.94

(A g

0.11

3.80

)

3.91

(Sb

5.84

B i

0.01

)

5.85

¡ (Fe

0.93

0.02

M n

0.06

)

1.01

(A g

0.03

3.97

)

4.00

(Sb

5.87

B i

0.03

)

5.90

¬ (Fe

0.99

0.01

M n

0.04

)

1.03

(A g

0.04

3.91

)

3.95

(Sb

6.12

B i

0.02

)

6.14

√ (Fe

0.94

0.00

M n

0.04

)

0.98

(A g

0.00

3.98

)

3.98

(Sb

6.12

B i

0 .03

)

6.15

ƒ (Fe

0.93

0.00

M n

0.04

)

0.97

(A g

0.04

3.89

)

3.93

(Sb

6.12

B i

0.02

)

6.14

NEW DATA ON “PLUMOSITE” AND OTHER SULPHOSALT MINERALS 397

appreciably closer to those of benavidesite (Oudin et al.
1982) than to either of the patterns for jamesonite. These
discrepancies are best attributed to the fact that the spectra
reported in the cited studies (Berry 1940; Garavelli 1958;

Oudin et al. 1982) lack the absolute precision of the present
investigation.

Cell parameters for our sample are calculated as a 15.71, b

19.10, c 4.03, also showing an apparent strong shift towards
benavidesite. Cell dimensions for jamesonite have been vari-
ously given as a 15.71, b 19.05, c 4.04 (Berry 1940); a 15.67,
b

19.06, c 4.02 (Hiller 1955); a 15.57, b 18.98, c 4.03 (Niize-

ki & Buerger 1957); and a 15.65 b 19.03, c 4.03 (Garavelli
1958). Oudin et al. (1982) gave the cell parameters for bena-
videsite as a 15.65, b 19.03, c 4.03 and a 15.74, b 19.14, c
4.06. These data contrast somewhat with those of Chang et
al. (1987) who gave a much narrower range in cell parame-
ters on synthetic jamesonite and benavidesite, Mn/(Mn+Fe)
= 0.7; a 15.74–15.75, b 19.17–19.14, c 3.99–4.04. The uncer-
tainties about the cell parameters of jamesonite, the differing
investigative methods and experimental conditions, as
well as possible errors in the various analyses, clearly do
not readily permit correlation between cell parameters
and degree of Mn substitution.

Jamesonite and parajamesonite

Zsivny & Náray-Szabó (1947) described a mineral from

Herja, found in the upper levels of the ălan vein. Composi-
tionally indistinguishable from „normal“ jamesonite, this
phase was distinguished by a significantly different X-ray
powder diffraction pattern. The mineral is reported to occur
as columnar crystals up to 8

2 mm in size, with rounded

faces and lacking good terminations. An orthorhombic or
lower symmetry was inferred. They named the mineral
parajamesonite, due to the apparent paramorphous relation-
ship with jamesonite. Koch et al. (1960) investigated jame-
sonite and „plumosite“ from Herja. Their study included a
number of samples from the same part of the mine as the
parajamesonite-bearing samples of Zsivny & Náray-Szabó
(1947), and which had a strong morphological resemblance
to the crystals in the original description. X-ray diffraction
patterns of these crystals, however, proved to be identical to
those of „normal“ jamesonite from elsewhere at Herja and
from other localities. Since that time, the discrete identity of
parajamesonite has been questioned in most standard miner-
alogical reference texts. No further samples of parajameso-
nite have been reported and it is particularly unfortunate that
the original small crystal of parajamesonite, which was the
subject of the 1947 description, was lost during the near to-
tal destruction by fire of the Magyar Nemzeti Museum,
Budapest (Náray-Szabó 1961). Furthermore, the parts of
the mine which yielded the original sample, which was
collected during the period 1915–1920, are no longer ac-
cessible, thus preventing further clarification. In the ab-
sence of unambiguous evidence that parajamesonite does
not exist, many mineralogists are prepared to believe that a
dimorph of jamesonite does exist at Herja, but that this is
exceptionally rare and restricted to a small part of the vein
system. The crystallographic studies reported here have
not been able to confirm the existence of parajamesonite in
the sample suite.

Plumosite,

Herja

Jamesonite

Benavidesite

(present study) (JCPDS-1CCD

13-461)

(Berry 1940)

(Oudin et al.

1982)

h k l

dcalc

020

9.552

9.47

9.57

120

8.161

8.09

8.17

220

6.065

6.01

6.05

6.08

130

5.901

5.87

5.91

310

5.048

5.03

5.05

5.06

240

4.080

4.06

4.07

4.09

400

3.926

3.90

3.92

3.93

410

3.845

3.82

3.85

150

3.712

3.70

3.72

121

3.587

3.59

340

3.528

3.51

3.53

250

3.436

100

3.43

100

3.43

100

3.44

100

430

3.342

3.33

3.34

3.35

311

3.196

3.20

060

3.184

3.17

231

3.153

3.14

3.166

160

3.120

3.11

510

3.099

3.10

3.103

350

3.086

3.091

041

3.078

3.08

141

3.035

3.01

260

2.951

2.94

2.93

2.956

411

2.825

2.83

2.831

331/530 2.819

2.813

2.821

421

2.658

2.656

2.742

360

2.720

2.714

2.725

341

2.682

2.675

421

2.658

2.656

2.677

261/180 2.367

2.361

2.36

2.356

640

2.295

2.290

2.29

280

2.285

2.289

171

2.242

2.236

2.23

2.249

470

2.241

2.245

560

2.236

720

2.184

2.187

380

2.173

730

2.116

2.109

541

2.185

090

2.127

461

2.126

2.130

631

2.104

551

2.104

631

2.060

371

2.061

081

2.054

2.047

2.061

181

2.032

2.026

740

2.030

2.034

660

2.022

002

2.013

2.030

471

1.943

721

1.942

0100

1.910

1.909 25(132)

580

1.894

490

1.867

191

1.857

481

1.826

751

1.756

831

1.716

5101

1.516

572

1.452

Table 6:

X-ray diffraction spectra.

398 COOK

and DAMIAN

Sulphur isotope geothermometry

S-isotope compositions of pyrite, galena, sphalerite and pyr-

rhotite within the Herja vein system are given in Table 7. The
data confirm the strong volcanic identity of the ores, with all
values lying within a relatively narrow field from -11.3 to
+3.1 ‰

S. Such values suggest that the sulphur in the ore-

forming fluids was derived from igneous sources at conditions
in which H

S was the dominant sulphur species (Rye & Ohm-

oto 1974). Some equilibration with the sedimentary host rocks
may have taken place, resulting in the shift towards lower val-
ues shown by some samples.

S-isotopic concentrations within coexisting pairs may be

used to determine temperatures of crystallization, assuming
that the minerals are pure, formed contemporaneously and in
equilibrium and that they did not re-equilibrate after crystalli-
zation. Given the more-or-less single stage of mineralization
as documented by relationships between the main sulphides in
the Herja deposit and the proven purity of the coarse-grained
sulphides used for analysis, these assumptions may be consid-
ered valid. Using the geothermometric calibration of Ohmoto
& Rye (1979), the following temperatures are obtained from
two coexisting pyrite-galena pairs: 417 ± 75

C (Vein 90, level

4) and 320 ± 70

C (Vein 50, level 4). These results are signifi-

cantly different to those of Pomárleanu (1971) who deter-
mined the following temperatures on the basis of fluid inclu-
sion data; 215–275

C for quartz, 190–200

C for calcite and

220–225

C for flourite. Borco et al. (1975) used the data to

argue in support of temperatures of about 300

C for pyrrhotite

and arsenopyrite crystallization, 250–280

C for sphalerite and

galena and temperatures below 215

C for the stibnite and sul-

phosalt parageneses. An explanation of this discrepancy may
be sought either in some disequilibration between sulphides in
the present study or that the fluid-inclusion based temperatures
of Borco et al. (1975) are too low; i.e. they represent tempera-
tures on the cooling path and do not reflect the true tempera-
ture maxima.

Acknowledgements:

The financial assistance of the Deutsche

Forschungsgemeinschaft is gratefully acknowledged. The
management of REMIN (Herja), and in particular, Crăciun
Adrian, the Mine Manager at the time of our fieldwork, are
gratefully thanked for their assistance during mine visits. The
helpful assistance of R. Hock with the X-ray diffraction analy-
sis, K.-P. Kelber with the photomicrographs and D.M. Radu
with preparation of Fig. 2 is appreciated. We also appreciate
the constructive reviews by M. Háber and E. Makovicky
which significantly helped to improve the manuscript.

References

Berry L.G., 1940: Studies of mineral sulpho-salts: II. Jamesonite

from Cornwall and Bolivia. Mineralogical Magazine, 40,
597–608.

Borco , M. & Lang, B., 1973: Le controle structural dans la metal-

logenese neogene des Monts Gutii. Rev. Roum. Geol. Geo-
phys. et Geograph., serie Geologie

, 17, 21–42.

Borco M., Lang B., Bostinescu S. & Gheorghita I., 1975: Neo-

gene hydrothermal ore deposits in the volcanic Gutái Moun-
tains. III. Dealul Crucii - Baiu district. A. Herja, Baia Sprie
and uior ore deposits. Rev. Roum. Geol. Geophys. et Geo-
graph., serie Geologie

, 19, 21–35.

Bracci G., Delena D., Orlandi P., Duchi G., & Vezzelani G., 1980:

Guettardite from Tuscany, Italy: a second occurrence. Cana-
dian Mineralogist

, 18, 13–15.

Chace F.M., 1948: Tin-silver veins of Oruro, Bolivia. Part II. Eco-

nomic Geology

, 43, 435–460.

Chang L.L.Y., Xilin Li & Chusheng Zheng, 1987: The jamesonite-

benavidesite series. Canadian Mineralogist, 25, 667–672.

Clark A.M. 1993: Heys Mineral Index, Third Edition, Chapman &

Hall, London, 852 pp.

Damian G.S., 1996: Studiul mineralogic i genetic al zăcământu-

lui polimetalic de la Herja.

Summary of Doctoral thesis, Edit-

ura Universitătii din Bucure ti, 1–25.

Edelstein O., Bernad A., Kovacs M., Crihan N. & Pécskay Z.,

1992: Preliminary data regarding the K-Ar ages of some erup-
tive rocks from Baia Mare Neogene volcanic zone. Revue
Roumaine de Geologie

, 36, 45–60.

Frizzo P. & Simone S., 1995: Diaphorite in the Pollone ore deposit

(Apuan Alps - Tuscany, Italy). European Journal of Mineral-
ogy

, 7, 705–708.

Garavelli C., 1958: Identitŕ fra „comuccite“ e jamesonite. Periodi-

co di Mineralogia

, 27, 207–214.

Ghiurca V. & Mo iu A., 1986: Curved jamesonite crystals from

Romania. Mineralogical Record, 17, 375–376.

Hiller J.E., 1955: Über den Falkmannit und seine Unterscheidung

von Boulangerit. Neues Jahrbuch Mineral. Monatsh., 1–10.

Hoffmann V., Trdlička, Z., Hulínský, V., Langrová A., & Arnoldová

V., 1977: Mineralogisch-chemisches Studium des Diaphorits
von Kutná Hora (ČSSR). Chemie der Erde, 36, 36–44.

Huber P. & Mure an I., 1996: Die Erzlagerstätte Herja. Lapis, 21,

27–34.

Jambor J., 1967: New lead sulfantimonides from Madoc, Ontario,

Parts 1 and 2. Canadian Mineralogist, 9, 7–24 and 191–200.

Koch S., Grasselly G. & Paděra K., 1960: Contributions to the

jamesonite problem. Szegedi Tudomanyegetem (Acta Univ.
Szeged, Hungary), Mineralogia-Petrographica

, 13, 17–32.

Lang B., 1979: The base-metals-gold hydrothermal deposits of

Baia Mare, Romania. Economic Geology, 74, 1336–1351.

Lang B., Edelstein O., Steinitz G., Kovacs M. & Halga S., 1994:

Ar-Ar dating of adularia - a tool in understanding genetic re-
lations between volcanism and mineralization: Baia Mare
area (Gutâi Mountains), Northwestern Romania. Economic
Geology

, 89, 174–180.

Lind I.L. & Makovicky E., 1982: Phase relations in the system Cu-

Sb-S at 200° C, 10

Pa by hydrothermal synthesis. Micro-

probe analyses on tetrahedrite - a warning. Neues Jahrbuch
für Mineralogie Abhandlungen

, 134–156.

Moëlo Y., Borodaev Y.S. & Mozgova N.N., 1983: Association twin-

nite-zinkénite-plagionite du gisement complexe ŕ Sb-Pb-Zn de
Rujevac (Yougouslavie). Bullétin de Minéralogie, 106, 505–510.

Mo iu A., Ghiurca V. & Târlea I., 1972: Aspecte paragenetice noi

in zâcâmintele de sulfuri din regiunea Baia Mare. Studia Uni-

Sample

Pyrite

Galena

Sphalerite

Pyrrhotite

GV-101

- 4.90

F-32

- 5.10

F-90-4

-8.01

-10.15

F-50-4

-8.23

-11.13

583-F-30

-7.36

Table 7:

Sulphur isotope data on sulphides from the Herja deposit

(

S ‰).

NEW DATA ON “PLUMOSITE” AND OTHER SULPHOSALT MINERALS 399

versitatis Babe -Bolyai

(Cluj-Napoca), Serie Geologia-Min-

eralogia (II/D), 17, 1, 11–19.

Mozgova N.N. & Bortnikov N.S., 1980: On non-stoichiometry of

the acicular lead sulphantimonides. In: Geochemija, Mineral-
ogija

, Nauka pub., Moscow, 126–138.

Mozgova N.N., Bortnikov N.S., Tsepin A.I., Borodaev Y.S.,

Vrublevskaja S.V., Vyalsov L.N., Kuzmina O.V. & Siftsov
A.V., 1983: Falkmanite, Pb

5.4

3.6

, new data and relation-

ship with sulphantimonites of lead (re-examination of type
material from Bayerland Mine, Bavaria) Neues Jahrbuch
Mineralogie Abhandlungen

, 147, 80–98.

Mozgova N.N., Efimov A.V., Nenasheva S.N., Golovanova T.I.,

Sivtsov,A.V., Tsepin A.I. & Dobretsova I.G., 1989: New data
on diaphorite and brongniardite. Zapiski Vsesoyuznogo Min-
eralogicheskogo Obshchestva

, 118, 47–63.

Mumme W., 1989: The crystal structure of Pb

5.05

(Sb

3.75

0.28

) S

10.72

boulangerite of near ideal composition. Neues Jahrbuch Min-
eral. Monatsh.

, 498–512.

Náray-Szabó I., 1961: Abstract and discussion of paper by Koch et

al. 1960. Zentralblatt für Mineralogie, Teil I (Kristallograph-
ie & Mineralogie), 273.

Niikeki N., & Buerger M.J., 1957: The crystal structure of jamesonite,

FePb

S14. Zeitschrift für Kristallographie, 109, 161–183.

Ohmoto H. & Rye R.O., 1979: Isotopes of sulfur and carbon. In:

H.J. Barnes (Ed.): Geochemistry of Hydrothermal Ore Depos-
its.

John Wiley & Sons, New York, 509-567.

Oudin E., Picot P., Pillard E., MoNlo Y., Burke E.A.J. & Zakrze-

wski M.A., 1982: La bénavidésite, Pb

(Mn,Fe)Sb

, un nou-

veau minéral de la série de la jamesonite. Bulletin de
Mineralogie

, 105, 166-169.

Petrulian N., 1934: Étude chalcographique du gisement de plomb et de

zinc de Herja (Transylvanie, Roumanie). Ann. Inst. Geol. Rom., 16.

Pomârleanu V., 1971: Geometria i aplicarea ei la unele minerale

din România. Editura Academiei Române, 1–158.

Rye R.O. & Ohmoto H., 1974: Sulfur and carbon isotopes and ore

genesis: A review. Economic Geology, 69, 826–842.

Szöke, A., 1968: Structura unor corpuri eruptive din regiunea Her-

ja (Baia Mare) i fenomenale de contact i autometamorfism
legate de ele. Studii et cercetari Geologie, Geofiz si Geogra-
phie, Serie Geologie

, 13, 1.

Uduba a G., Cristea C., Serbanescu A., Ghiurca V. & Uduba a S.,

1993: Fibrous sulphosalts in some ores of north Romania. Ab-
stract volume for the Third Geological Symposium

, Baia

Mare, October 1993, 3–4.

Uduba a G., Ilinca G., Marincea ., Săbău G. & Rădan S., 1992:

Minerals in Romania: the State of the Art 1991. Romanian
Journal of Mineralogy

, 75, 1–51.

Uduba a S., 1992: Contribution to the study of „Plumosite“ of Herja

(abstract). Romanian Journal of Mineralogy, 75 Suppl. 1, 46–47.

Zsviny V. & Náray-Szabó I., 1947: Parajamesonit, ein neues Miner-

al von Kisbánya. Schweiz. Mineral. Petrol. Mitt., 27, 183–189.