GeolCarp_Vol65_No6_419

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, DECEMBER 2014, 65, 6, 419—431 doi: 10.1515/geoca-2015-0003

Genesis of syntectonic hydrothermal veins in the igneous rock

of teschenite association (Outer Western Carpathians, Czech

Republic): growth mechanism and origin of fluids

TOMÁŠ URUBEK

, ZDENĚK DOLNÍČEK

and KAMIL KROPÁČ

Department of Geological Sciences, Faculty of Science, Masaryk University, Kotlářská 2, 611 37 Brno, Czech Republic;

urubek.tomas@seznam.cz

Department of Geology, Palacký University, Tř. 17. listopadu 12, 771 46 Olomouc, Czech Republic;

zdenek.dolnicek@upol.cz; kamil.kropac@upol.cz

(Manuscript received November 26, 2013; accepted in revised form October 2, 2014)

Abstract: Hydrothermal mineralization hosted by the Lower Cretaceous igneous rock of the teschenite association at
Jasenice (Silesian Unit, Flysch Belt, Outer Western Carpathians) occurs in two morphological types – irregular vein
filled by granular calcite and regular composite vein formed by both fibrous and granular calcite and minor chlorite,
quartz, and pyrite. Crosscutting evidence indicates that the granular veins are younger than the composite vein. The
composite vein was formed by two mechanisms at different times. The arrangement of solid inclusions in the marginal
fibrous zone suggests an episodic growth by the crack-seal mechanism during syntectonic deformation which was at
least partially driven by tectonic suction pump during some stages of the Alpine Orogeny. Both the central part of the
composite vein and monomineral veins developed in a brittle regime. In these cases, the textures of vein suggest the
flow of fluids along an open fracture. The parent fluids of both types of vein are characterized by low temperatures
(Th = 66—163 °C), low salinities (0.4 to 3.4 wt. % NaCl eq.), low content of strong REE-complexing ligands, and

and

C ranges of + 0.2/+12.5 ‰ SMOW and —11.8/—14.1 ‰ PDB, respectively. The parent fluids are interpreted as

the results of mixing of residual seawater and diagenetic waters produced by dewatering of clay minerals in the associ-
ated flysch sediments. The flow of fluids was controlled by tectonic deformation of the host rock.

Key words: Outer Western Carpathians, teschenites, syntectonic vein, fluid inclusions, stable isotopes, REE.

Introduction

Different types of mineralogically distinct hydrothermal veins
occur in all levels of the Earth’s crust. Their morphology, tex-
ture,  mineral  composition,  and  chemistry  offer  valuable  in-
formation about geological processes. In particular, veins are
useful  to  unravel  the  deformation  history  of  host  rocks
(Ramsay  &  Huber  1983;  Bons  &  Montenari  2005).  The
study of the shape and spatial orientation of veins can help to
determine the paleostrain orientation, while fluid inclusions
record  the  composition,  pressure,  and  temperature  of  vein-
forming fluids. A detailed description of internal vein micro-
structure  refining  the  paleostress  analysis  of  veins  presents
an  important  part  of  investigation  of  hydrothermal  veins.
Especially  fibrous  veins  can  record  the  opening  trajectories
of veins in greater detail (Hilgers & Sindern 2005).

The hydrothermal mineralization in the Silesian unit was

studied recently from the mineralogical and genetic points of
view  using  fluid  inclusion  microthermometry,  stable  iso-
topes, and trace elements (Urubek 2006, 2009; Polách 2008;
Polách et al. 2008; Urubek & Dolníček 2008; Urubek et al.
2009; Dolníček et al. 2010a,b, 2012). The results of previous
research  indicate  that  the  mineralogically  most  interesting
mineral associations occur in igneous rocks of the teschen-
ite association. Mineral assemblages involve mainly carbon-
ates,  chlorite,  quartz,  opal,  chalcedony,  and  rare  zeolites  or
sulphides.  These  post-magmatic  mineral  associations  were

formed from low-temperature ( < 50 to 220 °C) and low-salini-
ty (0.0 to 4.5 wt. % NaCl equiv.) fluids with elevated

values ( + 2 to + 14 ‰ SMOW). The parent fluids are inter-
preted as a mixture of magmatic waters (remaining after crys-
tallization of magma), diagenetic waters (produced by thermal
alteration of clay minerals in clastic sediments) and seawater.

This contribution focuses on the genesis of a fibrous vein

hosted  by  magmatic  rock  of  the  teschenite  association  found
at Jasenice. The microstructure, stable isotope, fluid inclusion
and  trace  element  studies  of  vein  minerals  provided  pilot  in-
formation about the physico-chemical conditions of formation
of syntectonic hydrothermal veins. Unlike the Polish and Slo-
vak  parts  of  the  Western  Carpathians  (Świerczewska  et  al.
2000; Milovský et al. 2003; Milovský & Hurai 2003), essen-
tially nothing is known about syntectonic veining in the Czech
(i.e. westernmost) segment of the Western Carpathians.

Geological setting and studied site

The Carpathians are a part of the European Alpine chain

created  by  convergence  and  collision  of  the  European  and
African  plates  (Golonka  et  al.  2000).  In  the  NE  part  of  the
Czech  Republic,  the  Outer  Carpathians  form  a  NW-verging
fold-and-thrust  belt  composed  largely  of  Upper  Jurassic-to-
Upper Oligocene flysch arranged into several nappes – Sub-
silesian,  Silesian  and  Magura  Nappes,  listed  from  tectonic

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foot-wall to hanging-wall (Fig. 1). The studied locality is sit-
uated in the Godula Development of the Silesian Unit which
consists  mainly  of  Upper  Jurassic-to-Upper  Oligocene  ma-
rine sedimentary rocks (Eliáš 1970; Stráník et al. 1993). The
basal  calcareous  turbidites  (Cieszyn  limestones  of  the  Late
Jurassic  age)  are  followed  by  black  calcareous  shales  alter-
nating  with  thin  layers  of  sandstones  (Hradiště  Formation)
passing  upwards  into  black  silicified  shales  (Veřovice  For-
mation).  Pelocarbonate  (mainly  siderite)  horizons  in  clay-
stone-rich cycles occur in some places. The subsidence and
spreading during the Lower Cretaceous was accompanied by
the extrusion of basic lavas giving rise to teschenites. In the
period from the Late Turonian to Early Eocene the sedimen-
tation of thick bedded coarse grained turbidites and fluxotur-
bidites (Godula Beds, Istebna Beds) took place. This period
of  intense  turbiditic  sedimentation  was  generally  connected
with Laramian tectonic movements that caused uplift of the
source  areas  associated  with  erosion  and  redeposition  of
clastic  sediments.  The  Oligocene  sequences  are  character-
ized by the presence of layers of dark organic-rich biogenic
silicite (Menilite formation). The shortening events related to
the Alpine Orogeny started in the Paleocene and continued up
to the early Late Miocene (Plašienka et al. 1997). During these
tectonic phases the whole sedimentary sequence including the

magmatic rocks was folded and thrusted towards the NW
onto the SE part Bohemian Massif.

The mafic quartz-free alkaline-to-subalkaline igneous rocks

of the teschenite association are products of a submarine Early
Cretaceous (Hauterivian—Barremian) magmatism. They form
hypoabyssal sills, submarine extrusions and pillow lavas and
are widespread in the area between Hranice in Moravia and
Bielsko-Biała in Poland. Rocks of the teschenite association
are  characterized  by  wide  variability  in  textures,  mineral
composition,  and  geochemistry  (Pacák  1926;  Šmíd  1962;
Kudělásková 1987; Hovorka & Spišiak 1988; Dostal & Owen
1998;  Lucińska-Anczkiewicz  et  al.  2002;  Spišiak  &  Mikuš
2008). Petrographically, they include teschenites, picrites, al-
kaline basalts, and monchiquites (Šmíd 1962).

The studied hydrothermal mineralization was found in

coarse-grained black-green massive picrite (Urubek 2009)
which forms a small natural outcrop (2

×1 m) in the bed of an

unnamed brook, about 1 km east from the center of the vil-
lage  of  Jasenice  near  Valašské  Meziříčí  (N 49°32.653’
E 17°57.803’,  altitude  592 m  a.s.l.).  Throughout  the  whole
outcrop,  the  picrite  is  strongly  altered.  In  thin  section  the
amygdaloid texture is observed with up to 3 mm large amyg-
dules  filled  by  calcite  and  chlorite.  The  rock  also  contains
phenocrysts of olivine, which is partially replaced by serpen-

Fig. 1. Geological position of the Jasenice locality in the Outer Western Carpathians flysch nappe system.

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tine and calcite. Brown amphibole, laths of plagioclase, and
flakes of biotite (which is often chloritized) constitute the
rock matrix.

Methods

The WDX electron microprobe analyses of minerals were

performed using Cameca SX-100 microprobe at the Masaryk
University in Brno. For carbonate and silicate minerals the
accelerating voltage of 15 kV, 20 nA beam current and beam
diameter of 10 µm (carbonates) and 5 µm (phyllosilicates),
respectively, have been used (Dolníček et al. 2010b; Kropáč
et al. 2012).

Fluid inclusions were investigated by means of petrography

and  microthermometry  in  standard  doubly  polished  wafers
and  cleavage  fragments.  The  distinguishing  of  primary  (P),
and secondary (S) inclusions was done according the criteria
given by Roedder (1984) and Shepherd et al. (1985). Micro-
thermometric  parameters  were  measured  using  the  Linkam
THMSG 600 stage at the Palacký University, Olomouc. The
temperature  of  final  homogenization  (Th)  and  melting  tem-
perature  of  ice  (Tm  ice)  were  measured.  The  stage  was  cali-
brated with inorganic standards and synthetic fluid inclusions.
The  reproducibility  is  within  0.1 °C  for  temperatures  be-
tween —56.6 and 0 °C, and within 1 °C for the temperature of
374.1 °C. The isochores were calculated using the computer
program Flincor (Brown 1989) with the equation of state by
Zhang & Frantz (1987).

For bulk chemical analyses, the carbonate samples weigh-

ing between 1 and 2 g were hand picked under a binocular mi-
croscope  and  then  pulverized  in  the  agate  mortar.  The  host
rock was powdered in an epicyclic mill and reduced in weight
by  quartering.  The  chemical  analyses  were  performed  in  the
ACME Analytical Laboratories, Vancouver, Canada. Aliquots
for analyses of the heavy metals were dissolved in hot (95 °C)
aqua regia and analysed using the ICP-ES method. Other de-
termined elements including refractory metals and rare earth
elements (REE) were analysed by ICP-MS in another sample
aliquot,  which  was  decomposed  using  LiBO

fusion fol-

lowed by leaching in diluted (5%) HNO

. Reproducibility of

the results is within 5—10 % based on analyses of standards.
The  REE  concentrations  were  normalized  to  C1-chondrite
according  to  values  determined  by  Anders  &  Grevesse
(1989). The Ce, Eu, and Yb anomalies were calculated using
the  following  equations  (McLennan  1989;  Monecke  et  al.
2002): Ce/Ce* = Ce

√(La

*Pr

), Eu/Eu* = Eu

√(Sm

*Gd

Yb/Yb* = Yb

√(Tm

*Lu

Stable isotope analyses were conducted in the laboratories

of the Czech Geological Survey, Prague, using a Finnigan
MAT 251 mass spectrometer. The conversion of carbonates
to CO

was done by reaction with 100% orthophosphoric

acid (McCrea 1950). The results of isotope analyses are con-
ventionally expressed in delta (

δ) notation as per mil (‰) de-

viation from commonly used standards (PDB, SMOW).
Uncertainty is better than ± 0.05 and ± 0.1 for

C and

respectively. The isotopic composition of the parent fluid
was calculated using the equations published by O’Neil et al.
(1969) and Deines et al. (1974).

Results

Vein types

Two types of vein texture were distinguished at the studied

locality: granular (V1) and composite (V2). Based on cross-
cutting evidence the V1 veins are younger than the V2 vein.

Granular veins (V1)

The outcrop is cut by seven hydrothermal veins 2 and

8 mm thick and up to several meters in length. A preferential
orientation  of  veins  was  not  observed:  they  strike  SW—NE,
SSW—NNE,  and  NNW—SSE  and  are  steeply  (60—80°)  dip-
ping  to  NW,  WNW,  and  WSW,  respectively  (Fig. 2).  The
tectonic striae have never been observed in the vein fill or on
the  contact  of  the  rock  and  vein.  No  remnants  of  host  rock
occur within the vein.

Granular veins are composed only of white calcite. In thin

section, the calcite grains are anhedral and slightly elongated
perpendicularly to the course of veins. The sizes of grains
are variable, ranging from 0.25 mm (marginal parts of veins)
up to 1 mm (center of veins). The undeformed (i.e. straight)
twinning lamellae have been sporadically observed in the
calcite grains.

Composite vein (V2)

Two composite extensional veins are undeformed and

their thickness ranges from 5 to 20 mm. The veins strike
NNW—SSE (dip ca. 20° to WSW) (Fig. 2) and are composed
of calcite, chlorite, quartz, and sporadic pyrite. The internal
fabric corresponds to the composite unitaxial syntaxial type

Fig. 2. The arc diagram of hydrothermal veins at the locality Jasenice.
Lower hemisphere of the Lambert’s projection.

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of fibrous veins (Ramsay & Huber 1983; Passchier & Trouw
1996) composed of a central part (median) and peripheral fi-
brous  parts.  The  median  has  a  constant  thickness  of  about
10 mm  and  is  formed  by  fine-grained  white  to  light  brown
calcite  containing  fragments  of  surrounding  rock.  These
fragments are situated mainly at the edge of the central part
of  the  vein.  The  marginal  part  adjacent  to  the  host  rock  is
characterized  by  development  of  fibrous  calcite,  which
shows the distinct growth zonality. The growth zones differ
in colour, which is milky white, light green or grey (Fig. 3).

Microscopic study demonstrates that calcite is the domi-

nant mineral phase. It completely fills the central part of the
vein (median) in the form of isometric anhedral grains. The
sizes of grains vary from 1.2 mm up to 3.7 mm. In the mar-
ginal  parts  calcite  forms  fibres  arranged  perpendicularly  to
the walls of the vein. Calcite fibres are slightly curved near
the  median  line.  The  thickness  of  individual  fibres  ranges
from 20 µm to about 0.5 mm, with a distinct increase of the
thickness  towards  the  vein-rock  interface.  In  the  case  of
greater thickness of fibres the twinning lamellae showing no
deformation are observed. The growth zoning of fibrous cal-
cite  is  sometimes  highlighted  by  the  presence  of  fragments
of  surrounding  rocks  (columns  of  brown  amphibole  and
flakes of chloritized biotite) and between the growing fibres
the  toothy  border  is  observed.  Fragments  of  host  rock  are
much  larger  than  the  fibre  diameter  and  are  arranged  as  in-
clusion  bands  parallel  to  the  vein  margin.  In  the  pressure
shadows  behind  these  rock  fragments,  calcite  aggregates
formed  by  isometric  grains  are  developed.  The  wall  rock
fragments are sometimes present on boundaries between fi-
bres of calcite. At the interface between the vein filling and
the surrounding rock narrow quartz selvage was found, con-
sisting  of  small  anhedral  quartz  crystals  that  grew  out  from
the  wall  rock.  The  width  of  this  selvage  is  quite  constant
(about 0.5 mm) and independent of that of the vein (Fig. 4a).

The EPMA analyses show that all the vein carbonate is

calcite. Chemical composition of fibrous calcite is very sim-
ple, showing up to 1.0 wt. % MgO, FeO or MnO. The calcite

located near the median has in addition an elevated content
of Mn (1.3 wt. % MnO).

Chlorite has been detected both in the median and in the

fibrous periphery of the vein. Chlorite of the median typically
forms  fan-shaped  aggregates  (Fig. 4c)  composed  of  fine
(100—200 µm)  flakes.  Chlorite  is  weakly  pleochroic  (light
yellow—light  brown-yellow)  and  shows  anomalous  inter-
ference  colours  in  green  hues.  The  occurrence  of  these
aggregates  is  associated  mainly  with  the  fragments  of  the
surrounding rock.

Chlorite in association with fibrous calcite forms elongated

individuals (ca. 100 µm in long), which are arranged parallel
to  calcite  fibres  and  exhibit  both  distinct  pleochroism  (co-
lourless  –  light  green)  and  anomalous  interference  colours
in green hues. Chlorite is typically associated with one of the
growth  zones,  which  has  macroscopically  green  colour.
Electron microprobe analyses were collected from chlorites
hosted in granular and fibrous calcite, and from those from
the  host  rock.  According  to  Melka’s  classification  (1965),
all the analysed chlorites belong to the pennine: Si = 3.89 to
4.78 apfu, Fe/(Fe + Mg) = 0.04—0.26 (Fig. 5).

The occurrence of pyrite is restricted only to the central

part of the vein, where it is enclosed by calcite. Pyrite forms
subhedral  to  anhedral  isolated  grains  about  0.5 mm  in  size,
occurring  in  the  form  of  hemispherical  aggregates  in  the
proximity of fragments of surrounding rock. The solitary py-
rites  sometimes  exhibit  growth  zonality  characterized  by
higher porosity in some incremental zones.

Quartz overgrows the walls of the vein where it forms the

selvage of almost constant thickness (see above) composed
of anhedral grains. Grains of quartz up to 0.5 mm large show
no evidence of fracturing but exhibit undulatory extinction.

Fluid inclusions

Fluid inclusions suitable for microthermometric analysis

were found in both V1 and V2 veins. In the case of V2 several
subsamples were taken: from the median (granular calcite I),

Fig. 5. Classification of chlorite from Jasenice (data points) in the diagram by Melka (1965) and a comparison with other mineralizations in the
Silesian Unit (outlined) hosted by both teschenite rock series (dashed line) and flysch sediments (full line). The comparative data are from
Urubek & Dolníček (2008), Dolníček & Polách (2009), Urubek et al. (2009), Dolníček et al. (2010a,b, 2012). a – chlorites from matrix of
igneous rock; b – chlorites from fibrous zone of composite vein; c – chlorites from granular zone of composite vein.

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peripheral  fibrous  parts:  white  (calcite II),  greenish
(calcite III),  calcite  associated  with  quartz  selvage  from  fi-
brous  growth  zones  (calcite IV);  and  calcite  from  the  mo-
nomineral granular – V1 vein (calcite V).

Calcites contain abundant primary and secondary fluid in-

clusions showing equant shapes and sizes ranging between 2
and 6 µm. The fluid inclusions are distributed relatively uni-
formly in the studied samples. The observed primary and
secondary inclusions are one-phase (L-only). Two-phase
(L + V) inclusions with essentially constant liquid-vapour ra-

Fig. 6. Results of microthermometry of primary fluid inclusions
from Jasenice. a – Histogram of homogenization temperatures
of  L + V  inclusions;  b  –  Histogram  of  melting  temperatures
of  last  ice;  c  –  Th-salinity  plot.  The  comparative  data  (white
field – vein carbonates cutting magmatic rocks in the Silesian
Unit; light grey field – diagenetic veins hosted by sedimentary
rocks  in  the  Silesian  Unit;  dark  grey  field  –  post-tectonic
veins hosted by sedimentary rocks in the Silesian Unit) are from
Świerczewska et al. (2000), Polách (2008), Polách et al. (2008),
Urubek  &  Dolníček  (2008,  2011),  Dolníček  &  Polách  (2009),
Urubek (2009), Dolníček et al. (2010a,b, 2012), and Jarmolowicz-
Szulc et al. (2012).

tios  (gaseous  phase  takes  ca.  5 vol. %)  are  less  frequent.
An exception is calcite V which contains mainly L + V and
less one-phase L inclusions. Most primary inclusions are
solitary,  show  regular  rounded  shapes,  sporadically  they
are  slightly  elongated  along  twinning  lamellae.  The  sec-
ondary fluid inclusions are arranged along healed micro-
fractures.  The  homogenization  temperatures  of  primary
fluid inclusions from calcite I and calcite V are character-
ized by slightly lower values (66—142 °C) than in the cases
of calcite II, III, and IV (103—163 °C). Generally, second-
ary  inclusions  showed  lower  homogenization  tempera-
tures  (about  100 °C).  Fluid  inclusions  have  generally
similar cryometric parameters. In all cases, the inclusions
freeze  at  temperatures  from  —34  to  —43 °C.  The  last  ice
melts at temperatures between —0.2 and —2.0 °C (Fig. 6a)
indicating bulk fluid salinities between 0.4 and 3.4 wt. %
NaCl eq. (Bodnar 1993) (Table 1). The cryometric data of
one-phase  inclusions  were  measured  after  heating  to  a
temperature exceeding 220 °C which led to stretching of
inclusions  and  subsequent  bubble  nucleation.  The  sec-
ondary  inclusions  have  generally  similar  microthermo-
metric parameters as the primary ones (Table 1).

The predominance of one-phase aqueous inclusions

could  indicate  very  low  trapping  temperatures  (below
50 °C) (Goldstein & Reynolds 1994), however, this is not
in  accordance  with  homogenization  temperatures  of  two-
phase inclusions ranging between 66 and 163 °C (Table 1).
The absence of vapour bubbles is often observed in smaller
( < 5 µm)  inclusions  implying  that  metastability  of  the
phase composition of the fluid inclusions could play a role.

There are no systematic differences between L-only

and L+V inclusions in their cryometric parameters, which
further support the idea about a metastable nature of the
liquid inclusions. The eutectic temperature was impossi-
ble to measure due to the small size of the inclusions.

Stable isotopes

The samples of carbonate were analysed for carbon and

oxygen isotope compositions from both V1 and V2 veins
(Table 2).

O values varying between —9.9 and —11.2 ‰

PDB and

C values between —12.5 and —11.5 ‰ PDB

were determined in the fibrous calcite of V2 vein. The
granular calcite from the median of V2 vein showed the
δ

O value of —4.5 ‰ PDB and the

C value of

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—10.3 ‰ PDB. One calcite from granular vein (V1) inter-
secting the composite vein yielded the

O value of

—10.9 ‰ PDB and the

C value of —11.4 ‰ PDB (Table 2).

Trace elements

The calcites from both the middle and margin of compos-

ite vein and one sample of host rock have been analysed for
selected trace elements (Table 3). The calcites from the com-
posite vein show increased Sr contents (983 and 1100 ppm)
which are slightly enriched in comparison with host rock

(845 ppm). Both samples show significantly lower contents
(31 and 72 ppm) of Ba in comparison with surrounding rock
(706 ppm).

The concentrations of rare earth elements (REE) are lower

in the calcite (

ΣREE=25 ppm) than in the host picrite

(

ΣREE=221 ppm). The chondrite-normalized patterns

(Fig. 7) follow similar trends in all samples characterized by
systematic decrease from La to Lu (LREE-enriched pattern).
Granular calcite from median exhibits a weak positive Eu ano-
maly (Eu/Eu* = 1.35) whereas other samples are without
Eu anomaly. All samples show weak negative Ce anomalies
(Ce/Ce* = 0.61—0.63).

Discussion

The growth mechanism

The texture of younger V1 veins suggests the transport of

fluid along an open fracture resulting in a blocky vein micro-
structure  combined  with  a  decrease  of  growth  rate  and  in-
crease  of  the  grain  size  towards  the  center  of  the  vein
(Hilgers et al. 2004; Hilgers & Sindern 2005). The observed
orientation  of  veins  corresponds  to  the  major  system  of
faults  in  this  area  that  formed  during  the  Late  Miocene
(Fig. 1) (Stráník et al. 1993).

The regular course of older composite V2 vein suggests

that the vein formation was initiated by brittle fracturing of
rock (Cosgrove 1993; Hilgers & Sindern 2005). The tension
veins  initially  formed  parallel  to  the  maximum  shortening
direction  which  corresponds  to  the  direction  of  the  vein
(Bons  2000).  The  formation  of  the  regional  folds  in  the
Outer  Carpathians  commenced  under  horizontal  compres-
sion  (Szczesny  2003),  which  corresponds  to  a  low  angle  of
dip of the vein. In addition, the axis of the largest stress (

)

was perpendicular to the fold axes and the smallest stress axis

Table 2: Carbon and oxygen isotope composition of calcites and

C and

O values of their parent fluids calculated for the given temperature.

Table 1: Results of fluid inclusion microthermometry.

Sample

FI type

Phase composition

Th (L+V) (°C)

Tf (°C)

Tm ice (°C)

Salinity (wt. % NaCl eq.)

Calcite I

L, rarely L+V

66–135

–39/–43

–0.2/–1.4

0.4–2.4

75–90

–38/–41

–0.4/–0.8

0.7–1.4

Calcite II

L, rarely L+V

110–163

–37/–41

–0.2/–2.0

0.4–3.4

Calcite III

L, rarely L+V

120–131

–38/–40

–0.2/–0.9

0.4–1.6

n.a.

–36/–42

–0.4/–0.6

0.7–1.1

Calcite IV

L, rarely L+V

103–148

–39/–41

–0.3/–1.5

0.5–2.6

L, L+V

110–125

–39/–42

–0.5/–1.4

0.9–2.4

Calcite V

L+V, rarely L

88–142

–34/–38

–0.5/–1.4

0.9–2.4

L, rarely L+V

93–115

–36/–39

–0.5/–0.9

0.9–1.6

P – primary fluid inclusions, S – secondary fluid inclusions, L – monophase liquid fluid inclusions, L+V – liquid—rich two phase fluid inclu-
sions (V – vapour phase), n.a. – not applicable.

Mineral

Hydrothermal solution

Sample

C ‰ (PDB) δ

O ‰ (PDB) δ

O ‰ (SMOW) T (°C)

O ‰ (SMOW)

C ‰ (PDB)

Calcite I

–10.3

–4.5

26.3

66/135

5.0/12.5

–12.1/–11.8

Calcite II

–12.5

–9.9

20.7

110/163

4.6/9.0

–14.1/–13.9

Calcite III

–11.5

–11.2

19.4

95/135

1.7/5.6

–13.1/–13.0

Calcite V

–11.4

–10.9

19.6

80/110

0.2/3.4

–13.1/–12.7

Fig. 7.  REE  chondrite-normalized  patterns  of  hydrothermal  calcites
and  host  magmatic  rock.  Normalization  values  are  from  Anders  &
Grevesse  (1989).  The  comparative  data  from  other  localities  in  the
Silesian Unit studied by Polách (2008), Polách et al. (2008), Urubek
& Dolníček (2008, 2011), Dolníček & Polách (2009), Urubek (2009),
and Dolníček et al. (2010a,b, 2012), are visualized as shaded fields.

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(

) retained a vertical position (Szczesny 2003). Moreover,

the direction of the V2 vein corresponds to the first event of
the tectonic evolution of the Outer Carpathians when the fold-
ing and thrusting were propagated to the NNW in the study
area (Botor 2006) and gave rise to the NNW-verging folds
and thrusts in the flysch rocks (Fig. 1). The compression in the
NNW-direction caused movement of the Silesian Unit in the
Czech segment (Födör 1991; Havíř 2000; Mlynář 2000). The
difference between the texture of the median zone and fibrous
margin of the V2 vein indicates distinctly different growth
mechanisms for the two parts of the tension vein.

Sample

Calcite I

Calcites II-IV

Host rock

30.8

706

<1.0

1.0

4.1

0.1

<0.1

0.2

<0.5

1.6

16.4

<0.5

<0.1

6.3

<0.5

2.7

<0.5

<0.1

13.7

<1.0

983

1100

845

<0.1

4.3

0.1

0.3

6.4

0.2

0.4

2.2

<5.0

237

0.1

0.5

<0.5

11.4

255

2.4

4.6

26.5

<0.1

1.2

1.5

43.7

0.9

4.3

170.8

<0.5

1.4

<0.1

0.1

<0.1

<0.5

0.01

<0.01

<0.1

0.5

<0.5

7.9

11.3

46.2

9.3

14.2

0.96

1.60

11.24

7.3

44.9

0.64

1.38

8.02

0.29

0.51

2.62

0.67

1.57

7.41

0.1

0.17

1.12

0.43

0.85

5.18

0.06

0.17

0.91

0.14

0.36

2.21

0.02

0.03

0.34

0.09

0.23

1.77

0.01

0.04

0.24

Σ REE

24.61

39.71

221.16

Yb/Yb*

0.90

1.01

0.85

Eu/Eu*

1.35

1.05

1.03

Ce/Ce*

0.61

0.63

0.91

Table 3: Trace element abundances in calcite and host rock samples
from Jasenice. All values are in ppm except for Au in ppb.

Calcite I – granular calcite from V2 vein, Calcites II—IV – fibrous
calcite from V2 vein.

The fibrous calcite. On the basis of linear bands of solid in-

clusions parallel to the vein wall, Ramsay (1980) proposed a
process  of  repeated  fracturing  and  sealing  –  the  so-called
crack-seal  mechanism.  The  regular  textural  periodicity  sug-
gests  veining  induced  by  hydraulic  fracturing  under  cyclic
changes in pore pressure. These crack-seal veins display saw-
tooth  shaped  grain  boundaries  between  adjacent  elongated
grains  with  preferred  growth  of  favourably  oriented  crystals.
Solid inclusions will be incorporated when a fracture reopens
after  crack  collapse  and  re-sealing.  This  happens  if  the  fluid
pressure increases to values larger than the minimum principal
stress oriented perpendicularly to the fracture wall and the ten-
sile strength of the rock. Under such conditions, crystals will
grow until fluid pressure drops due to fracturing and the void
collapses  (crack-seal  mechanism  with  incremental  growth).
This  may  result  in  a  feedback  system,  where  the  discharge
seals off the fluid pathways and fluid pressure repeatedly in-
creases  until  the  rock  is  resistant  to  stress.  Fibres  grow  in
a very narrow crack because the limited growth competition is
only compatible with growth on an essentially closed surface
(Hilgers & Urai 2002). The growth zonation is highlighted by
colour  zonation  of  calcite  and  sometimes  by  the  presence  of
fluid inclusions in calcite. Minor deformation of the veins has
occurred  either  during  vein  growth  or  after  vein  growth  as
vein calcite is twinned on the edge of the vein. Moreover, the
movements  during  vein  formation  are  indicated  by  slightly
curved calcite fibres containing minor mechanical twins show-
ing signs of tectonic deformation (Ramsay & Huber 1983).

Fibre curvature, growth direction and the type of host rock

vs.  vein  composition  are  consistent  with  unitaxial  syntaxial
growth  at  the  vein-wall  interface  (Durney  &  Ramsay  1973;
Ramsay  &  Huber  1983;  Passchier  &  Trouw  1996).  This  is
also supported by the microstructure of the polymineral ten-
sion vein, where growth is in one direction only at a single
unitaxial growth plane between vein and wall rock (Durney
& Ramsay 1973; Urai et al. 1991; Hilgers et al. 2001; Hilgers
& Urai 2002). The direction of growth is indicated by the in-
creasing width of the fibres towards the vein wall. Generally,
both fibrous marginal zones do not differ in the direction of
growth of calcite fibres.

Similarly, syntectonic fibrous veins tend to have a narrow

quartz selvage (Elburg et al. 2002; Hilgers & Urai 2002),
consisting of small quartz crystals that grew out from the
wall rock (syntaxial growth) which is consistent with our ob-
servation. The width of this selvage is quite independent of
the width of the vein.

Median zone. The difference in texture indicates that crys-

tal growth inside the median zone was driven by a different
mechanism  than  the  growth  of  the  fibrous  zones  on  both
margins of the vein (Bons & Montenari 2005). The shape of
grains  (elongated-blocky)  shows  that  growth  competition
was not suppressed during the precipitation of calcite. This is
indicated  by  the  fact  that  the  fracture  was  very  narrow  and
had a rough surface (Urai et al. 1991). The thickness of the
central zone of fracture (now formed by granular calcite) ini-
tiated  after  the  fibrous  stage  of  development  was  probably
not less than 10 mm (Hilgers & Urai 2002). This assumption
is  supported  by  the  constant  width  of  the  central  parts  of
veins  (about  1 cm).  Solid  inclusions  (angular  fragments  of

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surrounding rocks) are irregularly enclosed in calcite and do
not define any median growth plane of calcite grains. This
observation may indicate that fragments of surrounding rock
formed during initial opening of the crack.

P-T conditions of crystallization

Constant liquid-vapour ratios in primary L + V fluid inclu-

sions  in  calcite  suggest  trapping  of  the  homogeneous  fluid
phase.  Therefore,  the  measured  homogenization  tempera-
tures  are  the  minimum  possible  formation  temperatures
(Goldstein  &  Reynolds  1994).  The  true  trapping  tempera-
tures and pressures can be specified only if independent tem-
perature  and/or  pressure  estimates  are  available.  Since  the
aggregates of chlorite enclosed in both granular and fibrous
calcite from V2 vein show very high Si values often exceed-
ing the theoretical maximum of 4 apfu, chlorite compositional
geothermometers  (Cathelineau  1988;  Jowett  1991)  can  not
be used for determining the temperature of their formation.

However, as an upper possible temperature limit for syn-

tectonic V2 veins can be used the regional burial temperature
maximum  (ca. 160 °C)  indicated  by  vitrinite  reflectance
data,  illite  crystallinity,  and  fluid  inclusions  (Botor  et  al.
2006). The calculations show that these veins were probably
formed  in  low-pressure  conditions  ( < 1 kbar;  Fig. 8).  The
wide range of Th values observed for fibrous calcite may be

Fig. 8. Interpretation of P-T conditions for syntectonic veins at the Ja-
senice site and comparison with other mineralizations in the Silesian
Unit hosted by teschenite rock series (Dolníček et al. 2012 – dotted
line). The regional thermal maximum is from Botor et al. (2006). The
representative utmost isochores (solid lines – outliers neglected)
shown have been calculated using the computer program Flincor
(Brown 1989) with equation of state by Zhang & Frantz (1987).

due to variations in pressure which typically fluctuates be-
tween lithostatic and hydrostatic one during formation of the
crack-seal veins (Hurai et al. 2002). We can assume a de-
crease of temperature of parent solution during precipitation
of granular calcite from the V2 vein.

Salinity of fluids

The Th-salinity plot (Fig. 6c) documents mixing of two

fluid  endmembers  which  differ  in  temperature  and  salinity
for  calciteV.  The  presence  of  seawater  in  the  fluid  mixture
could  be  deduced  from  the  upper  limit  of  the  fluid  salinity
close  to  the  seawater  value  of  3.5 wt. %.  We  assume  that
seawater  retained  in  pore  system  of  sandstones  and  could
be released later into the cracks. The low-salinity fluid end-
member can be the diagenetic solutions derived from dehy-
dration of clay minerals. In the given geological setting the
activity of such low-salinity waters has been documented in
clay-rich sedimentary sequences (cf. Polách et al. 2008; Dol-
níček  &  Polách  2009).  The  high  Si  content,  Fe-depletion,
and  Al/(Al + Mg + Fe)  values  greater  than  0.35  in  chlorite
from  Jasenice  may  also  be  explained  by  the  crystallization
from  solutions  derived  from  argillaceous  rock  in  the  reduc-
ing conditions (Zhang et al. 2008).

Trace element signature of hydrothermal fluid

The low contents of elements incompatible with calcite

structure  (e.g.  Ga,  Zr,  Rb)  indicate  a  negligible  contamina-
tion of calcites by the host rock and/or vein silicate mineral
phases. High content of Sr (1100 ppm) in calcite samples can
be  explained  by  its  high  mobility  during  the  hydrothermal
process and co-precipitation with Ca-minerals. The observed
lower  content  of  Sr  in  granular  calcite  from  the  V2  vein
(983 ppm) can probably be related to the gradual cooling of
the hydrothermal solution and decrease of the rock/water ra-
tio during the later stage of development of the vein (Dickin
et al. 1984).

The low concentrations of REE in calcite from the tension

vein suggest relatively rapid precipitation of calcite (Möller
et al. 1997). The chondrite-normalized REE patterns (Fig. 6)
follow similar trends in all samples (host rock and vein cal-
cite)  characterized  by  systematic  decrease  from  La  to  Lu
with the exception of Ce and Eu, which are sensitive to Eh
changes    (Lee  et  al.  2003;  Dolníček  2005).  The  LREE  en-
richment of calcite similar to host rock indicates the low con-
tent  of  strong  REE-complexing  ligands  (F

—

, OH

—

or CO

2—

)

in  the  hydrothermal  solution  and  suggests  that  especially
sorption  processes  played  a  significant  role  during  incorpo-
ration of REE into calcite (Guy et al. 1999; Lee et al. 2003).
It  also  shows  local  REE  source  without  fractionation.  The
low  content  of  strong  REE-complexing  ligands  would  be
compatible  with  dehydration-related  fluids  originating  by
dewatering of clay minerals (Bau & Möller 1992) during dia-
genesis.  These  solutions  mixed  with  residual  marine  waters
and were passed through the body of igneous rocks along the
pressure gradient. When a fluid is percolated through the te-
schenite, the REE-complexing ligands (e.g. F and P) released
by breakdown of magmatogenic mineral phases were contin-

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uously removed and their concentration in the fluid phase
remains low (Dolníček et al. 2010a).

The negative Ce-anomaly observed in fibrous calcite can

indicate  a  seawater  component  in  the  fluid  (Hecht  et  al.
1999;  Wamada  et  al.  2007).  Alternatively,  the  presence  of
both negative Ce-anomaly and positive Eu-anomaly found in
granular calcite from median of composite vein suggest the
mixing  of  several  types  of  fluids  which  were  formed  under
various  redox  conditions  (Möller  et  al.  1991).  A  positive
Eu-anomaly  in  the  middle  part  of  a  composite  vein  can  be
explained  either  by  decrease  of  temperature  of  the  solution
under 200 °C or due to change of Eh in a hydrothermal solu-
tion (Bau & Möller 1992). Although the observed Th values
do not correspond to high-temperature conditions, we poten-
tially  can  not  exclude  a  short-term  activity  of  tectonically
generated  overheated  fluids  in  this  geological  situation  (cf.
Dolníček et al. 2012). Nevertheless the absence of a positive
Yb anomaly (Yb/Yb* = 0.9) (Bau & Möller 1992) combined
with  the  presence  of  a  negative  Ce-anomaly  can  indicate  a
lower temperature of the parent solution during precipitation
of  granular  calcite  from  the  V2  vein  (Wood  1990;  Bau  &
Möller 1992; Barker et al. 2006).

O and

C of the hydrothermal fluid

The fluid

O and

C characteristics have been calculated

from mineral

O and

C data and homogenization tem-

peratures measured in the respective samples (Table 2). The
calculated fluid

O values ranging from + 1.7 to + 9.0 ‰

SMOW are similar for all growth zones of the fibrous cal-
cite. The granular calcite from the median shows more posi-
tive fluid

O values between + 5.0 and + 12.5 ‰ SMOW.

The fluid

C values show a narrower range from —14.1 to

—13.0 ‰ PDB for fibrous calcite and —12.0 to —11.8 ‰ PDB
for granular calcite. The calcite from a younger granular vein
yielded ranges of + 0.2 to + 3.4 ‰ SMOW and —13.1 to
—12.7 ‰ PDB for fluid

O and

C, respectively. It

should be noted that the use of pressure-uncorrected Th val-
ues leads to underestimated fluid

C and especially

values for syntectonic calcites. However, the qualitative in-
terpretation of the source of their fluids (see below) will not
be affected.

The variable

O values may be compatible with mixing

of  two  (or  more)  fluids  with  contrasting  isotope  composi-
tions  (e.g.  residual  seawater  residing  in  the  pore  system  of
sandstones  with  a  near-zero

O value (Sheppard 1986)

could mix with water characterized by highly positive

values. In the given geological setting, the diagenetic waters,
derived from surrounding sedimentary rocks, thus probably
represent the best candidate to explain both the low fluid sa-
linity and elevated

O values. The observed elevated

values in a paragenetically younger granular calcite of com-
posite vein (V2) could be explained by a pronounced isoto-
pic exchange of oxygen between rocks and fluid phase
(Sheppard 1986; Torres-Alvarado et al. 2011). Last but not
least the generally high

O values of fluids may also origi-

nate during interaction of fluids with isotopically heavy sedi-
mentary carbonates (Dolníček et al. 2010a). The lower

values of the fluids in the youngest phases (V1 veins) can be

explained by either decreasing temperature of the fluid-rock
interaction or mixing with isotopically light surface waters
(i.e. meteoric or marine water) in the latest stage of the min-
eralizing process (Sheppard 1986). The calculated

C val-

ues of the fluid phase indicate a mixed carbon source, most
likely from both “carbon of the homogenized Earth’s crust”
(

C = —5 to —8 ‰ PDB) averaged from various crustal

sources during fluid evolution and carbon derived from oxi-
dized organic matter (

C = —20 to —30 ‰ PDB). The negli-

gible variations in fluid

C values can be explained by

rock-buffered fluid system (Hoefs 1997).

Comparison with other hydrothermal systems

The available data on fluid salinity from Jasenice are com-

parable to those from previously studied hydrothermal min-
eralizations in the Silesian Unit (Fig. 6c). Most post-magmatic
mineral associations were formed from low-temperature ( < 50
to  170 °C)  and  low-salinity  (0.0  to  4.5 wt. %  NaCl  equiv.)
fluids  (Polách  2008;  Urubek  &  Dolníček  2008,  2011;
Urubek 2009; Dolníček et al. 2010a,b, 2012). The only ex-
ception  is  early  post-magmatic  stage  which  was  formed
from  high-temperature  (390—510 °C)  and  high-salinity
(47—57 wt. % salts) fluids released during crystallization of
magma  (Dolníček  et  al.  2010a).  The  hydrothermal  veins
hosted by sedimentary rocks formed from low-temperature
(mostly  60—155 °C,  exceptionally  up  to  220 °C)  and  low-
salinity  (1.0-3.6  wt.  %  NaCl  eq.)  fluids  (Świerczewska  et
al.  2000;  Polách  2008;  Polách  et  al.  2008;  Dolníček  &

Fig. 9. Oxygen and carbon isotopic composition of hydrothermal
fluids from Jasenice (data points) in comparison with other locali-
ties in the Silesian Unit (outlined; full line – veins hosted by igne-
ous rocks; dashed line – veins hosted by sedimentary rocks;
coarsely dashed line – diagenetic veins; thin dashed line – postec-
tonic veins). The comparative data are from Polách (2008), Urubek
& Dolníček (2008), Dolníček & Polách (2009), Urubek (2009), and
Dolníček et al. (2010a,b, 2012).

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Polách 2009; Jarmolowicz-Szulc et al. 2012). The studied
syntectonic veins show slightly lower fluid

C values in

comparison with other veins in the studied area, while the
range of

O values is almost identical (Fig. 9). This obser-

vation  indicates  that  carbon  originating  from  either  earlier
(i.e.  post-magmatic)  mineralizations  and/or  from  organic
matter  participated  in  formation  of  the  syntectonic  veins.
The REE patterns of hydrothermal vein carbonates are simi-
lar to the other carbonate-bearing mineralizations in the Sile-
sian  Unit  (Fig. 7).  Recycling  of  at  least  some  components
from  earlier  mineralizations  confirm  the  rock-buffered  na-
ture of the hydrothermal system during syntectonic veining.

Conclusion

Hydrothermal mineralization from the locality of Jasenice

is located in an outcrop of picrite in two morphologic types:
(i)  granular  veins  without  preferred  spatial  orientation  and
(ii) composite unitaxial syntaxial syntectonic veins. Granular
veins  0.2  to  2 cm  thick  are  composed  only  of  isometric
grains  of  calcite.  The  composite  tension  vein  is  asymmetri-
cally  banded.  It  is  composed  mainly  of  calcite  and  minor
chlorite  (pennine),  quartz,  and  pyrite.  The  vein  was  formed
by two mechanisms. The peripheral fibrous parts are the re-
sult of episodic hydraulic fracturing followed by the healing
of  the  microfractures  by  calcite  (crack-seal  mechanism)  re-
sulting  in  a  fibrous  texture.  By  contrast,  the  middle  part  of
the  composite  vein  composed  of  granular  calcite  originated
in  a  brittle  regime,  when  fluids  most  likely  moved  along  a
fracture in a pre-existing vein.

Generation of the parent fluids is probably connected with

Tertiary  deformation,  folding  and  thrusting  of  the  whole
Silesian Unit. The fluids were derived by mixing of seawater
residing in pores of clastic sediments and diagenetic waters
produced by dewatering of clay minerals in associated flysch
sediments.  The  REE  and  isotopic  studies  suggest  the  exist-
ence of a geochemically more or less closed system buffered
by the host rock sequence. The fluid movement was mainly
driven by the tectonic suction pump which continuously sup-
plied ions into the fluid. The vein-forming components were
transported  mainly  by  diffusion  to  their  deposition  site
(Sibson  et  al.  1975).  Similarly,  fibrous  crystals  growing  in
small  cracks  (due  to  prevention  of  the  growth  of  competi-
tion) do not favour large-scale fluid conduits. It is more likely
that  they  indicate  pervasive  flow  or  diffusion  (Bons  2000;
Oliver & Bons 2001; Elburg et al. 2002).

Hydrothermal minerals precipitated from low-salinity (0.4 to

3.4 wt. % NaCl eq.) and low-temperature (Th = 66 to 163 °C)
aqueous solutions. The REE data indicate that the fluid was
poor in strong REE-complexing ligands and that redox po-
tential changed during crystallization.

The above described interpretations of fluid origin are

comparable to the results obtained from other types of hy-
drothermal mineralization hosted by teschenite rock series in
the Silesian unit as well as those hosted by flysch sediments
implying similar sources of hydrothermal solutions in both
environments. The existing data moreover suggest a continu-
ous evolution of the fluid system in the given area from sedi-

mentation and post-magmatic alteration of associated te-
schenite intrusions through diagenesis, rock deformation
during the Alpine Orogeny, up to the post-orogenic faulting.

Acknowledgments: The study was supported by the GAČR
Project 205/07/P130. P. Gadas (MU Brno) is thanked for as-
sistance during microprobe work. The isotope analyses con-
ducted  by  I.  Jačková  and  Z.  Lněničková  (ČGS  Praha)  are
highly  appreciated.  V.  Hurai,  A.  Świerczewska,  and  han-
dling  editor  J.  Lexa  are  thanked  for  detailed  reviews  which
helped to improve the initial draft of the manuscript.

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