GEOLOGICA CARPATHICA
, APRIL 2017, 68, 2, 119 – 129
doi: 10.1515/geoca-2017-0010
www.geologicacarpathica.com
Genetic aspects of barite mineralization related to rocks
of the teschenite association in the Silesian Unit,
Outer Western Carpathians, Czech Republic
JAKUB JIRÁSEK
1
, ZDENĚK DOLNÍČEK
2
, DALIBOR MATÝSEK
3,1
and TOMÁŠ URUBEK
2, 4
1
Institute of Geological Engineering, Faculty of Mining and Geology, Vysoká škola báňská — Technical University of Ostrava,
17. listopadu 15/ 2172, 708 33 OstravaPoruba, Czech Republic;
jakub.jirasek@vsb.cz
2
Department of Geology, Faculty of Science, Palacký University, 17. listopadu 1192/12, 771 46 Olomouc, Czech Republic
3
Institute of Clean Technologies for Mining and Utilization of Raw Materials for Energy Use, Faculty of Mining and Geology,
Vysoká škola báňská — Technical University of Ostrava, 17. listopadu 15/ 2172, 708 33 OstravaPoruba, Czech Republic
4
Department of Geology and Pedology, Mendel University of Agriculture and Forestry, Zemědělská 1, 613 00 Brno, Czech Republic
(Manuscript received January 28, 2016; accepted in revised form November 30, 2016)
Abstract: Barite is a relatively uncommon phase in vein and amygdule mineralizations hosted by igneous rocks of the
teschenite association in the Silesian Unit (Western Carpathians). In macroscopically observable sizes, it has been
reported from 10 sites situated only in the Czech part of the Silesian Unit. Microscopic barite produced by the hydro
thermal alteration of rock matrix and also by the supergene processes is more abundant. We examined four samples of
barite by mineralogical and geochemical methods. Electron microprobe analyses proved pure barites with up to
0.038 apfu Sr and without remarkable internal zonation. Fluid inclusion and sulphur isotope data suggests that multiple
sources of fluid components have been involved during barite crystallization. Barite contains primary and secondary
aqueous allliquid (L) or less frequent twophase (L+V) aqueous fluid inclusions with variable salinity (0.4–2.9 wt. %
NaCl eq.) and homogenization temperatures between 77 and 152 °C. The highersalinity fluid endmember was probably
Cretaceous seawater and the lowersalinity one was probably diagenetic water derived from surrounding flysch sediments
during compaction and thermal alteration of clay minerals. The δ
34
S values of barite samples range between –1.0 ‰ and
+16.4 ‰ CDT suggesting participation of two sources of sulphate, one with a nearzero δ
34
S values probably derived
from wall rocks and another with high δ
34
S values being most probably sulphate from the Cretaceous seawater. All results
underline the role of externally derived fluids during postmagmatic alteration of bodies of rock of the teschenite
association.
Keywords: Silesian Unit, teschenite, barite, fluid inclusions, stable isotopes.
Introduction
For more than 150 years, the Podbeskydí (Beskydy Piedmont)
area lying at the eastern edge of the Czech Republic near the
border with Poland and Slovakia (Fig. 1) has been known for
the occurrence of a special group of mostly alkaline basaltic
igneous rocks, which are often referred to as teschenites (sensu
Hohenegger 1861), rocks of the teschenite association (Šmíd
1978; Kudělásková 1987), or teschenitepicrite formation
(Hovorka & Spišiak 1988). In southern Poland, where small
bodies of these rocks also occur, the term rocks of the Cieszyn
magmatic province (Smulikowski 1930, 1980; Włodyka 2010)
is used. Picrite (Tschermak 1866) and teschinite sensu stricto
(Rosenbusch 1887) were described for a first time in the
Podbeskydí Piedmont area.
One of the specific features of teschenites is intense hydro
thermal alteration of primary rockforming minerals to a mix
ture of zeolites (analcime), phyllosilicates, and carbonates
(Pacák 1926; Smulikowski 1930; Šmíd 1978; Dolníček et al.
2010a,b, 2012; Urubek et al. 2014; Kropáč et al. 2015). In
addition, cementation of fissures and vesicles by hydrothermal
minerals gave rise to abundant hydrothermal veins and
amygdules. Recent studies (Dolníček et al. 2010 a,b; Dolníček
et al. 2012; Urubek et al. 2014; Kropáč et al. 2015) revealed
that multiple stages of hydrothermal activity occurred in this
rock environment. The most important event was early
postmagmatic alteration, which took place immediately after
solidification of the host rock, when fluid circulation was
allowed due to heat flow associated with the host intrusion
(e.g., Dolníček et al. 2010 a,b). Later alteration events occurred
during subsequent deeper burial (Dolníček et al. 2012;
Kropáč et al. 2015) and thrusting during the Alpine Orogeny
(Dolníček et al. 2010 a; Urubek et al. 2014).
Along with carbonates, chlorites, zeolites, quartz, fluorite,
glauconite, and sulphide minerals, barite is also observed in
the hydrothermal paragenesis of veins and amygdules. In
macro scopically observable sizes, it is relatively uncommon
mineral, reported from 10 sites situated only in the Czech part
of the Silesian Unit (Table 1). Both amygdule and veinhosted
examples have been described, but the exact geological posi
tion of some historical finds is unknown today (cf. Table 1).
Barite in microscopic size, as crystals and grains up to 50 μm
in size and filling of fissures, is abundant (Fig. 2). The origin
of such barite is connected to the hydrothermal alteration of
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JIRÁSEK, DOLNÍČEK, MATÝSEK and URUBEK
GEOLOGICA CARPATHICA
, 2017, 68, 2, 119 – 129
rock matrix (Matýsek 2013) and also with supergene pro
cesses (Matýsek, unpublished data).
The aim of this study is to characterize the most important
teschenitehosted occurrences of barite mineralogically and
genetically. We have studied four archive samples in terms
of fluid inclusions and stable isotopes. Barite is a sink for
sulphate dissolved in the hydrothermal fluids and its isotopic
composition together with the nature of the parent fluids
enclosed in fluid inclusions are useful tracers of the origin
of fluids (e.g., Majzlan et al. 2016). Moreover, these inde
pendent data can further help to verify the reliability of
existing interpretations of sources of hydrothermal fluids.
Magmatic, marine, and diagenetic fluid sources have
been suggested by previous works in this area (cf. Pacák
1926; Šmíd 1978; Dolníček et al. 2010 a,b, 2012; Urubek et
al. 2014).
Geological setting
Eastern Moravia and Silesia belong to an area built up by
nappe units of the Outer Western Carpathians, thrusted over
the SE part of the Bohemian Massif during the Tertiary
(Fig. 1). Predominantly flysch sediments of the Upper
Jurassictouppermost Palaeogene were transformed during
several stages of the Alpine Orogeny into discrete tectonic
units. Based on the superposition, the following units were
distinguished in the studied area: the Subsilesian Unit, Silesian
Unit, and Magura Unit (Menčík et al. 1983; Fig. 1). The Sile
sian Unit, which hosts the study sites, consists of two basic
facial developments. The Godula facies represents sediments
of the ocean floor, while the Baška facies is considered to be
deposited on a frontal continental slope. The differentiation is
likely to have occurred during the Cenomanian. The occur
rence of igneous rocks of the teschenite association is almost
exclusively bound to the sediments of the Hradiště Formation
(terminology by Eliáš et al. 2003) belonging to the lower part
of the Silesian Unit; they are also rarely situated in the
Vendryně Formation and in the Těšín Limestones, underlying
the Hradiště Fm. (e.g., Włodyka 2010). The Hradiště Forma
tion is composed of typical flysch sediments and consists of
unmetamorphosed calcareous claystones, siltstones, and sand
stones (Eliáš 1970) of the Late Valanginian to Early Aptian
age (Skupien & Vašíček 2002).
Fig. 1. Schematic geological map of the occurrences of rocks of the teschenite association in the Czech part of the Podbeskydí area (compiled
after Czech Geological Survey 2014 and Matýsek & Jirásek 2016). Position of the studied localities: 1 — Skotnice, 2 — Palačov, 3 — Kojetín,
4 — Hodslavice.
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BARITE MINERALIZATION OF THE TESCHENITE ROCKS IN THE SILESIAN UNIT
GEOLOGICA CARPATHICA
, 2017, 68, 2, 119 – 129
Rocks of the teschenite association usually form sills, rarely
dykes or lava pods (Matýsek & Jirásek 2016). In the Czech
part, subaquatic effusive types such as lava flows, pillow
lavas, tuffs, and tuffites are relatively common (Šmíd 1978).
Shallow subvolcanic intrusions prevail over effusive types
(Szopa et al. 2014). Radiometric dating carried out by
LucińskaAnczkiewicz et al. (2002; Ar–Ar method) and Szopa
et al. (2014; U–Pb method on apatite) gave ages of 120.4 –
122.3 Ma and 103.0 –126.5 Ma, respectively. These dates are
consistent with palaeontological evidence from the syngenetic
sediments of the Hradiště Fm. (Valanginian to Aptian; Vašíček
1972; Eliáš et al. 2003; Skupien & Pavluš 2013).
Rocks of the teschenite association are characterized by
widely variable mineral composition, variable structural and
textural features, and extremely variable intensity of post
magmatic alterations. There are many classification schemes
of these rocks (Pacák 1926; Smulikowski 1930; Šmíd 1978;
Hovorka & Spišiak, 1988; Włodyka 2010). The most frequent
rock types include teschenites, picrites, monchiquites, and
alkali basalts; gradual transitions are often observed among
them (Machek & Matýsek 1994). Leucocratic components in
these rocks are represented by alkali feldspars, plagioclase,
analcime, zeolites, and nepheline, mafic minerals comprise
pyroxene (Tirich diopside and hedenbergite, rarely augite)
and amphibole (usually kaersutite). Olivine (Fo
~90
) occurs
mainly in picrites and Tirich biotite was identified in lampro
phyric varieties. Accessory minerals include pyroxenes of
aegirineaugite series, fluorapatite, Tirich magnetite or
Crrich spinels (in picrites), titanite, sulphides, and others.
Postmagmatic alterations are a characteristic feature of rocks
of the teschenite association. Šmíd (1978) described a variety
of alterations which include analcimization, chloritization,
smectitization, serpentinization, and carbonatization.
Rocks of the teschenite association belong to basic,
alkalinetosubalkaline rocks with elevated concentrations of
TiO
2
, P
2
O
5
, alkalis, and incompatible trace elements (REE, Zr,
Nb, Y, Ba, and Sr — Dostal & Oven 1998). The contents of Ba
are abnormally high and highly variable. From published data
(30 analyses; Włodyka 2010; Dostal & Oven 1998; Dolníček
et al. 2010 a,b, 2012), the contents of Ba vary between 125 and
2164 ppm. Unpublished XRF data of the authors (50 analyses
performed by D. Matýsek) revealed <600 – 4614 ppm Ba.
Ba does not provide statistically significant correlations with
other components of rocks, which may be related to the occur
rences of Baminerals or with the redistribution of this ele
ment during the postmagmatic alterations (cf. Fig. 2). There
are known mineralogical occurrences of harmotome, hyalo
phane, Barich alkali feldspars with up to 8 wt. % BaO
(Włodyka 2010), slawsonite with variable content of celsiane
component, celsiane (Matýsek & Jirásek 2016), witherite, and
barite (Table 1).
The origin of rocks of the teschenite association is related to
shortterm rifting of the continental crust (Oszcypko 2004;
Ivan et al. 1999; Hovorka & Spišiak 1993; Narebski 1990).
Dostal & Owen (1998) suggested that the magma was of
mantle origin and its composition resembles that of ocean
island basalts and some continental alkaline basalts.
Material and methods
We have studied four samples of barite hosted by rocks of
the teschenite association from locations illustrated in Fig. 1.
The sample from Skotnice originated from an abandoned
quarry on the western slope of the Hončova hůrka Hill
(N 49° 39.590’ E 18° 09.180’), which had exploited strongly
Locality
Description
References
Choryně
One small crystal of barite was found in a vug of a magmatic rock in the bed of the Bečva River near the village of
Choryně.
Matýsek, unpublished
data
Hodslavice
Small white barite crystals occur in thin veinlets hosted by altered picrite in the Palackého lom Quarry
Bobková (1936),
Burkart (1953)
Kojetín (1)
Small free fragments of milky white barite are from a creek springing between the Požáry and Hory Hills, near junction
with a creek springing below the Kojetín village.
Melion (1855),
Šmíd et al. (1964)
Kojetín (2)
Fragments of barite, coarse grained calcite, and chalcedony covered by quartz crystals were found on a tilth near the
southern margin of the village. Host rock is a strongly altered amygdaloid volcanite.
Šmíd et al. (1964)
Kunčice pod
Ondřejníkem
Calcite veins hosted by amphibole fourchite in the Maralův lom Quarry contain younger witherite which is corroded and
overgrown by small tabular crystals of barite.
Kudělásek et al. (1989)
Nový Jičín (1)
Tabular barite crystals overgrowing drusy quartz are from the Gimpelberg Hill (today called Hýlovec Hill) situated
between the Bludovice and Žilina villages. A fragment of barite was also found in a creek south of the Hill.
Melion (1855),
Sapetza (1864),
Šmíd et al. (1964)
Nový Jičín (2)
Fragments of barite together with calcite and analcime were found at the locality Čerťák, south of the town of Nový
Jičín, in the vicinity of water reservoir Čerťák
Tschermak (1860)
Palačov
Barite was found in the Pavlíkův lom Quarry. No further details are given by original author.
Kučera (1926)
Příbor
Barite was found on building site of new by–pass road of the town of Příbor. It represents one of the youngest phases
filling the fissures in a rock of teschenite association.
Kynický (2010)
Skotnice
Colorless, bluish, white or grey–white crystalline aggregates of barite occur in central parts of carbonate geodes in
strongly altered picrite in the quarry at the Hončova hůrka Hill. Also found as monomineral fillings of amygdules up to
several kg in weight. The 2–4 mm big tabular crystals were found in a small veinlet in picrite.
Rusek & Valošek (1968),
Dolníček et al. (2010b)
Table 1: An overview of todate known occurrences of barite mineralization hosted by igneous rocks of the teschenite association in
the Silesian Unit.
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JIRÁSEK, DOLNÍČEK, MATÝSEK and URUBEK
GEOLOGICA CARPATHICA
, 2017, 68, 2, 119 – 129
altered effusive picrite (Rusek & Valošek 1968). Abundant
amygdules and fissures are filled up by lowtemperature
hydrothermal mineralization formed by dolomite, magnesite,
siderite, quartz, calcite, fluorite, aragonite, glauconite, chlorite,
sulphides, and barite (Dolníček et al. 2010 b; Kropáč et al.
2015). The studied sample is a fissile piece of greywhite
barite overgrowing calcite in a spherical geode representing
the filling of an amygdule. The sample was collected in 1966
by D. Matýsek.
The sample from Palačov is from the collection of the
Moravian Museum in Brno (inventory number A1579). It is
a speci men described by Kučera (1926), from whose collec
tion it originated. Locality is the Pavlíkův lom Quarry situated
in a “dyke/sill of a picritic igneous rock”. At present the
quarry does not exist, but according to Frejková (1952) it can
approxi mately be situated at the coordinates N 49° 33.000’
E 17° 56.000’. The studied sample is a whitegrey fissile piece
of barite without associated minerals or wall rock.
The sample from Kojetín is from the collection of the
Moravian Museum (inventory number 2684). It is probably
a sample collected by Melion (1895), but no additional infor
mation on its geological position is available today. Samples
of identical appearance were collected by Šmíd et al. (1964) at
a site with the coordinates N 49° 33.555’ E 17° 58.306’. At this
place and on the slope above, there are outcrops of various
types of amygdaloid picrites, monchiquites, tuffs, and tuffites
(Šmíd 1978). The studied sample is a white fissile piece of
barite without other minerals or wall rock.
The sample from Hodslavice came from the Moravian
Museum (inventory number 15477). It is a find described
by Bobková (1936) and Burkart (1953), which originated
from the Palackého lom Quarry (N 49° 33.127’ E 18° 01.669’)
Fig. 2. Backscattered electron (BSE) images of microscopic barites (white) on a fracture surfaces. A — barite impregnation in rock matrix,
fourchite, Bruzovice; B — isometric euhedral barite crystals, amygdaloidal picrite, Baška; C — barite impregnation in rock matrix, fourchite,
Kunčice pod Ondřejníkem; D — barite coating on prismatic apatite crystal, teschenite, Řepiště near Paskov.
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BARITE MINERALIZATION OF THE TESCHENITE ROCKS IN THE SILESIAN UNIT
GEOLOGICA CARPATHICA
, 2017, 68, 2, 119 – 129
situated in a body of picrite to diabase picrite (Klvaňa 1897;
Pacák 1926; Šmíd 1978). The studied sample is formed by
white tabular crystals of barite up to 2 mm in size, developed
on a fissure of host picrite. Barite is associated with minor
calcite.
The chemical composition of barite was studied with
an electron microprobe Cameca SX 100 at the Faculty of
Science, Masaryk University in Brno (analyst R. Škoda).
The following conditions were used: wavelengthdispersive
analysis, accelerating voltage 15 keV, beam current 10 nA,
beam diameter 5 μm. Well defined minerals and synthetic
phases were used as standards: Sr (Lα, SrSO
4
), Na (Kα, albite),
Si (Kα, sanidine), Mg (Kα, Mg
2
SiO
4
), P (Kα, fluorapatite),
Ca (Kα, fluorapatite), Fe (Kα, almandine), Mn (Kα, spessar
tine), Ba (Lα, barite), S (Kα, barite), Cl (Kα, vanadinite),
Pb (Mα, vanadinite), Zn (Kα, gahnite). The counting time on
each peak was 20 s in the case of major elements and 40 s in
case of minor elements, the same as on the background.
Fluid inclusions were investigated by means of petrography
and optical microthermometry in cleavage fragments of barite.
The distinguishing of individual genetic types of fluid inclu
sions was made according the criteria given by Roedder
(1984) and Shepherd et al. (1985). Inclusions were checked
for the presence of petroleum under ultraviolet (UV) radiation
at 365 nm excitation wavelength. Microthermometric para
meters were measured using the Linkam THMSG 600 stage
mounted on the Olympus BX51 microscope (Palacký Univer
sity, Olomouc). The temperature of final homogenization
(Th), freezing temperature (Tf), and melting temperature of
ice (Tm
ice
) were measured. The stage was calibrated between
–56.6 and 374.1 °C with inorganic standards and synthetic
fluid inclusions. The reproducibility is within 0.1 °C for
tempe ratures between –56.6 and 0 °C, and within 1 °C for
temperature up to 374.1 °C. The cryometric data of one phase
L inclusions were measured after heating to a temperature of
200 °C which led to stretching of inclusions and subsequent
bubble nucleation. Salinity of fluids was calculated from
measured Tm
ice
values according to Bodnar (1993).
Sulphur isotope analyses of barites were conducted in the
laboratories of the Czech Geological Survey in Prague,
using a Finnigan MAT 251 mass spectrometer (analyst
Z. Lněničková). The SO
2
gas for isotope analysis was pro
duced by heating of powdered barite with a SiO
2
+V
2
O
5
mix
ture (Ueda & Krouse 1987) at 1050 °C in vacuum. Results of
isotope analyses are conventionally expressed in delta (δ)
notation as per mil (‰) deviation from the commonly used
CDT standard. Uncertainty involving the whole analytical
procedure is better than ± 0.3 ‰.
Results
Chemical composition of barite
Electron microprobe analyses (Table 2) revealed that all
samples belong to rather pure barite without remarkable
internal zonation. The highest contents of strontium were
found in samples from Hodslavice (up to 0.038 apfu) and
Kojetín (up to 0.010 apfu). The contents of calcium were with
one exception (sample Hodslavice containing up to 0.014 apfu)
always below the detection limit of the microprobe. In addi
tion, some samples contained slightly elevated contents of
zinc (up to 0.005 apfu), iron (up to 0.002 apfu), and silica (up
to 0.006 apfu). The concentrations of other analysed elements
(Mg, Cl, P, Na) were always below the detection limits.
Fluid inclusions
Fluid inclusions suitable for microthermometric analysis
were found in all studied barite samples. Samples contain
abundant primary fluid inclusions showing essentially con
stant sizes ranging between 5 and 8 µm. They are mostly
solitary with regular rounded isometric shapes, sporadically
slightly elongated inclusions occur along growth zones. At
room temperature, the studied primary inclusions are one
phase (Lonly) in most cases. Twophase (L+V) inclusions
with essentially constant liquidvapour ratios (gaseous phase
takes about 5 to 10 vol. %) are less frequent and are spatially
associated with Linclusions (Fig. 3a). Frequent irregular flat
tened or isometric secondary inclusions arranged in trails
along healed microfractures (Fig. 3a) usually reach very small
sizes (up to 3 µm). Somewhat larger secondary inclusions are
present in the sample from Palačov (Fig. 3b) and contain
aqueous solution only (Linclusions). No fluorescence has
been observed in the UVmicroscope in any type of fluid
inclusion.
The homogenization temperatures of twophase primary
fluid inclusions range between 77 and 152 °C (Table 3,
Fig. 4a). However, a narrower variability (within ca. 30 °C) is
usually observed for most samples with an exception of fluid
inclusions from Skotnice which range within 55 °C (77 to
133 °C).
Fluid inclusions have generally similar cryometric parame
ters (Table 3, Fig. 4). In all cases, the inclusions freeze at tem
peratures between –38 and –43 °C. The frozen fluid inclusions
usually remain colourless, sometimes slight darkening of the
inclusion content is observed. Eutectic melting as well as salt
hydrate melting was never observed due to observation
complications caused by small sizes of the fluid inclusions.
The last ice melts at temperatures between –0.2 and –1.7 °C
(Table 3, Fig. 4b) indicating bulk fluid salinities between 0.4
and 2.9 wt. % NaCl eq. There is no systematic difference
between associated L+V and Lonly primary inclusions in
terms of their salinity. The secondary inclusions showed
slightly higher Tm values (–0.3 to –1.0 °C) than the primary
inclusions in the same sample (Table 3, Fig. 4b).
Sulphur isotopes
The following δ
34
S values have been determined for the stu
died barite samples: Hodslavice –1.0 ‰ CDT, Skotnice +8.0 ‰
CDT, Kojetín +14.2 ‰ CDT, and Palačov +16.4 ‰ CDT.
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, 2017, 68, 2, 119 – 129
Discussion
Fluid inclusions
Constant liquidvapour ratios in primary L+V fluid inclu
sions confirmed by rather narrow ranges of measured homo
genization temperatures suggest trapping of a homogeneous
fluid phase in the studied baritehosted fluid inclusions. There
fore, the measured homogenization temperatures of primary
inclusions should represent the minimum possible formation
temperatures (Goldstein & Reynolds 1994). Moreover, narrow
ranges of Th values together with often welldefined trends in
the ThTm
ice
plot (Fig. 4c) in individual samples imply good
preservation of fluid inclusions in barite host which is usually
reported to be very sensitive to postentrapment leakage and
stretching of fluid inclusions (e.g., Ulrich & Bodnar 1988). In
contrast, the occurrence of numerous onephase aqueous
inclusions would indicate very low formation temperatures
not exceeding ca. 50 °C (Goldstein & Reynolds 1994) which
contradicts the information given from L+V inclusions. The
absence of vapour bubbles is often observed in smaller inclu
sions (with sizes below about 6 µm) implying that metastabi
lity of the bubble nucleation could play a role. The idea about
a metastable nature of the liquid inclusions is supported by the
fact that there are no systematic differences in cryometric
parameters of Lonly and associated L+V inclusions.
Different trends for different samples can be observed in the
ThTm
ice
plot (Fig. 4c). Fluid inclusions from Palačov, Kojetín,
Skotnice
Palačov
Kojetín
Hodslavice
Spots
6
7
6
5
average
max.
min.
average
max.
min.
average
max.
min.
average
max.
min.
BaO
65.26
65.62
65.04
65.02
65.65
64.39
64.50
64.90
64.09
63.33
64.57
62.80
SrO
0.04
0.06
0.00
0.09
0.11
0.04
0.39
0.43
0.35
1.32
1.69
0.19
CaO
0.00
0.01
0.00
0.01
0.02
0.00
0.01
0.02
0.00
0.13
0.34
0.05
ZnO
0.04
0.10
0.00
0.03
0.09
0.00
0.05
0.16
0.00
0.03
0.10
0.00
FeO
0.03
0.06
0.00
0.01
0.03
0.00
0.01
0.04
0.00
0.01
0.10
0.00
SiO
2
0.07
0.16
0.00
0.00
0.14
0.00
0.04
0.12
0.00
0.06
0.09
0.00
SO
3
33.75
34.31
33.17
33.94
34.49
33.28
33.84
34.55
33.15
34.50
34.65
34.15
Total
99.20
99.14
98.85
99.37
Ba
2+
1.005
1.016
0.994
0.999
1.011
0.980
0.993
1.006
0.976
0.959
0.974
0.950
Sr
2+
0.001
0.001
0.000
0.002
0.003
0.001
0.009
0.010
0.008
0.030
0.036
0.004
Ca
2+
0.000
0.001
0.000
0.000
0.001
0.000
0.001
0.001
0.000
0.005
0.014
0.002
Zn
2+
0.001
0.003
0.000
0.001
0.003
0.000
0.001
0.005
0.000
0.001
0.003
0.000
Fe
2+
0.001
0.002
0.000
0.001
0.001
0.000
0.000
0.001
0.000
0.000
0.001
0.000
Si
4+
0.003
0.006
0.000
0.000
0.001
0.000
0.002
0.006
0.000
0.002
0.003
0.000
S
6+
0.995
1.002
0.990
0.999
1.005
0.994
0.997
1.002
0.992
1.000
1.003
0.997
Table 2: Average chemical composition of barite (oxides in wt. %) and recalculation of coefficients of empirical formulae to 4 atoms of
oxygen.
Fig. 3. Microphotographs of fluid inclusions hosted by the studied barite. a — A group of L and L+V primary (P) fluid inclusions neighbouring
with trails of very small secondary (S) fluid inclusions in the sample from Kojetín. b — Larger flat irregularly shaped originally allliquid
secondary inclusions after overheating to 200 °C which resulted to stretching of most inclusions and nucleation of vapour bubbles. Sample from
Palačov.
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and Hodslavice define diagonal or subverti
cal trends which have to be interpreted in
terms of mixing of fluids with different
salinities and/or temperatures. By contrast,
the sample from Skotnice yielded a subhori
zontal distribution which can be interpreted
in terms of (i) mixing of two fluids with the
same salinity and different temperatures;
(ii) changes of temperature of a single fluid;
(iii) changes of pressure of a single fluid;
(iv) postentrapment damage to fluid inclu
sions caused by neckingdown; (v) a combination of the above
mentioned possibilities. The variations of pressure seem to be
unlikely alone to explain the observed variability in Th values,
because decrease from 130 °C to 75 °C requires increase of
pressure by 1.3 kbars (modelling in the Flincor software using
an isochore calibration by Zhang & Frantz 1987), which is
unlikely for a postmagmatic mineralization developed in
a body of effusive picrite which originated in a marine basin
with a depth more than the CCD (cf. also Dolníček et al.
2010 b). Larger variability in Th values has been reported for
some amygdulehosted aqueous fluid inclusions from Skotnice
by Dolníček et al. (2010 b); these authors presupposed damage
to fluid inclusions by neckingdown. In any case, various
trends observed for individual samples clearly suggest mixing
of contrasting types of fluids related to the local low
temperature hydrothermal systems.
The lower salinity of secondary fluid inclusions suggests
decrease of salinity of hydrothermal fluids during evolution of
the hydrothermal system. Such a trend is very characteristic
for lowtemperature postmagmatic hydrothermal minerali
zations hosted by teschenites in the Silesian Unit (e.g.,
Dolníček et al. 2010 a,b; Urubek et al. 2014).
Sulphur isotopes
The wide observed range of δ
34
S values of the studied barite
(–1.0 to +16.4 ‰ CDT) can be interpreted by involvement of
either multiple sources of sulphur or various processes affec
ting fractionation of sulphur isotopes. Fig. 5 summarizes
available data on isotopic composition of possible sources of
sulphur. Sulphidic minerals disseminated in teschenites
showed δ
34
S values between –7.4 and +2.4 ‰ CDT, whereas
sulphides from postmagmatic vein and amygdule minerali
zations hosted by teschenites have δ
34
S values between –23.6
and +6.8 ‰ CDT; the isotopic composition of sulphur from
flysch sediments of the Hradiště Fm. adjacent to teschenites
has not been studied yet. The tescheniterelated sources are
not heavy enough to explain the observed highest δ
34
S values
of the studied barites. The increase of δ
34
S values of sulphate
dissolved in a hydrothermal fluid can be potentially caused by
partial reduction of sulphate to H
2
S resulting in shift of δ
34
S
values of residual sulphate due to kinetic isotope effects
(Hoefs 2005). However, two of three principal mechanisms of
sulphate reduction operate at temperatures which are out of
the range suggested by our fluid inclusions (inorganic sulphate
Sample
Genesis
Phase
composition
Th (°C)
Tf (°C)
Tm
ice
(°C)
Salinity
(wt. % NaCl eq.)
Hodslavice
Primary
L, L+V
92–118
–39/–43
–0.5/–1.2
0.9–2.1
Kojetín
Primary
L, L+V
103–140
–38/–43
–0.3/–1.7
0.5–2.9
Palačov
Primary
L, L+V
120–152
–39/–41
–0.8/–1.3
1.4–2.2
Palačov
Secondary
L
n.a.
–38/–42
–0.3/–1.0
0.5–1.7
Skotnice
Primary
L, L+V
77–133
–39/–43
–0.2/–0.5
0.4–0.9
Fig. 4. Graphical presentation of results of microthermometry of fluid
inclusions in the studied barites. a — Histogram of homogenization
temperatures of L+V fluid inclusions. b — Histogram of melting
temperatures of last crystal of ice. c — Th vs. salinity plot. Outlined
are comparative data from the Silesian Unit (Urubek et al. 2014 and
references therein): white field refers to postmagmatic teschenite
hosted carbonaterich mineralizations, light grey field is syntectonic
tesche nitehosted mineralization, and dark grey field are diagenetic
and posttectonic vein mineralizations hosted by sedimentary rocks.
Table 3: Results of fluid inclusion microthermometry on teschenitehosted barites from
the Silesian Unit. n.a. — not applicable
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GEOLOGICA CARPATHICA
, 2017, 68, 2, 119 – 129
reduction: above ca. 250 °C; bacterial sulphate reduction:
below ca. 80 °C; Hoefs 2005; Desrocher et al. 2004). Thermo
chemical reduction of sulphate by organic matter cannot
be a dominant source because of the lack of higher hydro
carbons in the parent fluids which is indicated by the absence
of fluorescence in an UVmicroscope. Therefore, our data
rather suggest involvement of an additional source of isotopi
cally heavy sulphate, which can most probably be found in
seawater sulphate showing δ
34
S values of ca. +16 ± 2 ‰ CDT
during the Lower Cretaceous period (Strauss 1997;
Hoefs 2005).
Genetic model
Crystallization of barite occurred from aqueous fluids with
salinities ranging between 0.4 and 2.9 wt. % NaCl eq. In the
given setting, such wide variability in fluid salinity was very
common during postmagmatic hydrothermal activity and
cannot be explained by a single fluid source (cf. Dolníček et
al. 2010 a,b; Dolníček et al. 2012; Urubek et al. 2014).
The available fluid inclusion data (cf. Fig. 4c) suggest partici
pation of at least two types of fluid. The lowsalinity fluid end
member cannot be considered to be meteoric water because of
submarine position of the host igneous rocks. Similarly,
lowsalinity fluid cannot have a magmatic source with respect
to the rather shallow nature of the basin (above CCD) which
results in production of highsalinity fluids during the final
stages of magmatic crystallization (cf. Cline & Bodnar 1991).
The likely source of lowsalinity fluid can be found in diage
netic waters, produced by compactional and thermal dewate
ring of clayey sediments spatially and temporarily associated
with the rocks of teschenite association. Such diagenetic fluids
are frequently described from both teschenite and sediment
hosted minerogenetic environments in this area (Dolníček et
al. 2010 a,b; Dolníček et al. 2012; JarmolowiczSzulc et al.
2012; Urubek et al. 2014). The highersalinity fluid end
member can be found in either magmatic fluids (with salinities
reaching up to several tens of wt. % NaCl eq. in the given area;
cf. Dolníček et al. 2010a) or seawater (with salinity of
3.5 wt. % NaCl eq.). With respect to the rather low tempera
tures of the fluid mixture requiring substantial previous
cooling of the host igneous rocks (which was dominantly
mediated by fluids circulating along fractures), we suggest
that seawater was the crucial source of salinity in the hydro
thermal fluid. Nevertheless, the contribution of the higher
salinity fluid decreased with time, as indicated from decreasing
salinity of secondary fluid inclusions. Barium can be leached
from rocks along the fluid pathways (from teschenites and/or
clayey sediments). Adamová (1983) states that barium
contents range between 146 and 560 ppm in the sediments of
the Hradiště Formation. The source of sulphate can domi
nantly be found in Cretaceous seawater (in case of high δ
34
S
values) or rocks (in the case of nearzero δ
34
S values; again
possibly derived from both teschenites and/or clastic sedi
ments). Both Ba and sulphate can be brought by the individual
fluid endmembers and mixing of compositionally different
fluids (having often different temperatures) at the site of depo
sition resulted in barite crystallization. A possible genetic
scenario is illustrated in Fig. 6.
Conclusions
Barite is a relatively uncommon phase in vein and amygdule
parageneses hosted by igneous rocks of the teschenite associa
tion in the Czech part of the Silesian Unit. The available data
suggest that multiple sources of fluid components have been
involved during barite crystallization. Fluid inclusions reveal
mixing of at least two fluid endmembers differing in salinity
and sometimes also in temperature. The highersalinity end
member was probably Cretaceous seawater and the lower
salinity one was probably diagenetic water derived from
surrounding flysch sediments during compaction and thermal
alteration of clay minerals. The wide range of δ
34
S values of
Fig. 5. Comparison of δ
34
S values of the studied barites and possible sources of sulphur. Comparative data are from Strauss (1997),
Hoefs (2005), Urubek & Dolníček (2008), and Dolníček et al. (2010 b, 2012). Unpublished data of the authors are also included.
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BARITE MINERALIZATION OF THE TESCHENITE ROCKS IN THE SILESIAN UNIT
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barite also suggests mixing of two sources of sulphate, one
with nearzero δ
34
S values probably derived from wall
rocks (either teschenites or sediments) and another with
high δ
34
S values (up to +16 ‰ CDT) being most probably
sulphate from the Cretaceous seawater. These findings
underline the role of externally derived fluids during post
magmatic alteration of bodies of rock of teschenite association
and the significance of leaching of specific wall rocks for
mine ral paragenesis preci pitating from circulating fluids.
Acknowledgements: This study was made possible by
financial support from the grant projects No. SP2016/12
and IGA UP PrF_2015_014, which were financed by the
Ministry of Education, Youth and Sports of the Czech
Republic. Part of the analytical work was performed using
equipment that was financed by the project “Institute of
Clean Technologies for Mining and Utilization of Raw
Materials for Energy — Sustainability Project”, reg. no.
LO1406, financed by the Ministry of the Education, Youth and
Sports of the Czech Republic. The authors are grateful to the
staff of the Department of Mineralogy and Petrography,
Moravian Museum in Brno, for allowing access to the
histo rical samples. Analytical data carried out by R. Škoda
(MU Brno) and Z. Lněničková (ČGS Praha) are highly
appreciated. The authors are grateful to Juraj Majzlan and an
anonymous reviewer for their constructive comments and
suggestions, which substantially improved the quality of
the manuscript.
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