GeolCarp_Vol65_No5_387

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, OCTOBER 2014, 65, 5, 387—399 doi: 10.2478/geoca-2014-0022

Petrology and geochemistry of a peridotite body in Central-

Carpathian Paleogene sediments (Sedlice, eastern Slovakia)

MATÚŠ KOPPA

, FRIEDRICH KOLLER

and MARIÁN PUTIŠ

Department of Mineralogy and Petrology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,

Slovak Republic; putis@fns.uniba.sk; koppa@fns.uniba.sk

Department of Lithospheric Research, University of Vienna, Althanstrasse 14, Vienna, Austria; friedrich.koller@univie.ac.at

(Manuscript received February 12, 2014; accepted in revised form June 5, 2014)

Abstract: We studied representative samples from a peridotite body situated NE of Sedlice village within the Central-
Carpathian Paleogene sediments in the Central Western Carpathians. The relationship of the peridotite to the surrounding
Paleogene sediments is not clear. The fractures of the brecciated peridotite margin are healed with secondary magnesite
and calcite. On the basis of the presented bulk-rock and electron microprobe data, the wt. % amounts of mineral phases
were calculated. Most of calculated “modal” compositions of this peridotite corresponds to harzburgites composed of
olivine ( ~ 70—80 wt. %), orthopyroxene ( ~ 17—24 wt. %), clinopyroxene ( < 5 wt. %) and minor spinel ( < 1 wt. %).
Harzburgites could originate from lherzolitic protoliths due to a higher degree of partial melting. Rare lherzolites contain
porphyroclastic 1—2 mm across orthopyroxene (up to 25 wt. %), clinopyroxene ( ~ 5—8 wt. %) and minor spinel
( < 0.75 wt. %). On the other hand, rare, olivine-rich dunites with scarce orthopyroxene porphyroclasts are associated with
harzburgites. Metamorphic mineral assemblage of low-Al clinopyroxene (3), tremolite, chrysotile, andradite, Cr-spinel to
chromite and magnetite, and an increase of fayalite component in part of olivine, indicate low-temperature metamorphic
overprint. The Primitive Mantle normalized whole-rock REE patterns suggest a depleted mantle rock-suite. An increase in
LREE and a positive Eu anomaly may be consequence of interactive metamorphic fluids during serpentinization. Similar
rocks have been reported from the Meliatic Bôrka Nappe overlying the Central Western Carpathians orogenic wedge since
the Late Cretaceous, and they could be a potential source of these peridotite blocks in the Paleogene sediments.

Key words: peridotite, petrology, geochemistry, Slovakia.

Introduction and brief geological background

The presence of meta-ultramafic rocks within (meta)silici-
clastic sediments may open new insights on the mobility of
serpentinized mantle fragments within accretionary and col-
lision wedges and their interaction with continental crust
(e.g. Brandon 2004; Scambelluri et al. 2004).

Representative samples were collected for study from a

500

×300 m surface occurrence of an ultramafic body to the

NE  from  Sedlice,  which  forms  a  smaller  ridge  in  the  Šariš
Highlands  marked  on  the  map  as  the  “Dunitová  Skalka”
(“dunite stone” of Cambel 1951; Hovorka et al. 1985). It is
situated N of the zone of pre-Carboniferous metamorphosed
complexes  intruded  by  Variscan  granitoids  in  the  Branisko
and  Čierna  hora  Mountains,  in  the  eastern  part  of  the  Cen-
tral-Carpathian  Paleogene  flysch  belt  (Marschalko  1966;
Plašienka et al. 1997), in the middle of basal sandstone and
conglomerate  beds.  This  zone  belongs  to  the  Central  West-
ern  Carpathians  (Plašienka  et  al.  1997).  The  relationship  of
the  serpentinized  peridotite  body  to  the  surrounding  Paleo-
gene sediments is not clear. The body may be a member of a
buried  Mesozoic  complex  covered  by  transgressive  Paleo-
gene  sediments,  or  an  olistolith  within  these  sediments  (Ho-
vorka et al. 1985). The geological position is shown in Fig. 1.

The peridotite body near Sedlice was the subject of inter-

ests and studies of different aspects in the past. Cambel
(1951) reported enstatite dunites based on microscopic and

optical  identification  of  rock-forming  minerals.  The  rocks
with increased Cpx content associated with Spl were classi-
fied  as  spinel  lherzolites  (Cambel  1951;  Fejdi  &  Kolník
1988;  Stankovič  et  al.  2007).  These  rocks  contain  a  certain
amount  of  opaque  minerals,  usually  in  paragenesis  with
spinel. Awaruite, millerite or pentlandite have been reported
in  the  ultramafic  rocks  from  Sedlice  by  Kantor  (1955)  and
Rojkovič  (1985).  The  spinel-group  and  ore  minerals  were
studied  by  Kantor  (1955),  Rojkovič  (1985),  Rojkovič  et  al.
(1978, 1979, 1982), Spišiak et al. (2000) and Mikuš & Spi-
šiak  (2007);  serpentine-group  minerals  by  Hovorka  et  al.
(1980,  1985);  geochemistry  by  Hovorka  (1977);  geother-
mometry and geobarometry by Fejdi & Kolník (1988), Rad-
vanec  (2000);  exsolved  pyroxenes  by  Stankovič  et  al.
(2007);  mesoscopic  structures  by  Jaroš  et  al.  (1981),  and
tracing  the  spatial  distribution  of  the  body  by  geophysical
methods was performed by Gnojek & Kubeš (1991). Despite
the previous results, evolution of the body placed within the
Central Carpathian Paleogene sediments remains unclear or
“exotic”.

This paper reports the results of mineralogical-petrologi-

cal, and geochemical study of the Sedlice ultramafic body in
the Western Carpathians in the territory of eastern Slovakia
based on the study of the mineral (EMPA) and whole-rock
(XRF and ICP MS) chemical compositions of representative
samples. The mantle and crustal evolution, and tectonic ori-
gin of these rocks is discussed.

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Materials and methods

X-ray fluorescence spectrometry was used for whole-rock

major oxide and also some trace element concentrations con-
tained in rock samples. In order to obtain representative ma-
jor and trace element analyses, the rock samples were
crushed in jaw mill and ground to the finest powder possible
in an agate swing mill. Subsequently, the fused beads were
prepared using Li

after the sample powders were dried

at  110 °C  and  heated  at  950—1050 °C  to  determine  loss  on
drying and ignition. Major and trace element concentrations
were determined on fused beads and pressed powder pellets
with a wavelength dispersive X-ray fluorescence spectrome-
ter  (PHILIPS  PW  2400)  at  the  Department  of  Lithospheric
Research,  University  of  Vienna.  The  fused  beads  were  cast
using a Philips Perl X3 automatic bead machine. A rhodium
anticathode was employed for the XRF analyses.

Trace element contents (including rare earth elements –

REEs) were analysed by ICP-MS at the Department of Gen-
eral and Analytical Chemistry, Montan-University Leoben. In
total  0.1 g  of  fine  grained  sample  was  sintered  with  sodium
peroxide (purity 95%) to achieve complete digestion of all sil-
icate and spinel mineral phases (Meisel et al. 2002). Measure-
ments were performed with an Agilent 7500 ce ICP-MS with
and without He collision cell mode. The International Associ-
ation  of  Geoanalysts  (IAG)  Candidate  reference  material
MUH-1,  a  highly  depleted  serpentinized  harzburgite  from
Kraubath, Styria, Austria (Burnham et al. 2010), was used for
quality control purposes. The preceding sodium peroxide sin-
tering and acid digesting (37% HCl) followed the procedures
of Meisel et al. (2002). A solution with very accurately known
concentrations of Ge, In and Re (1 µl/ml) was employed as a
reference material. The machine used was a standard quadru-
pole ICP-MS Agilent Technologies HP4500 with a v-groove

Fig. 1.  Tectonic  sketch  of  basic  tectonic  units  and  basement  com-
plexes in the Slovak Western Carpathians. OWC – Outer Western
Carpathians;  CWC  –  Central  Western  Carpathians,  divided  into
the  Tatric,  Veporic  and  Gemeric  basement-cover  complexes  (Late
Cretaceous tectonic units) overlain by small (often less than kilome-
ter size) Meliatic fragments (according to Biely et al. 1996) with lo-
cation  of  the  Sedlice  ultramafic  body  in  the  Central  Carpathian
Paleogene sediments. TM – Tatra Mountains; bottom figure: Geo-
logical map of studied locality. Black arrow with rectangle represents
the position of the ultramafic body. Legend: 1, 2– Quaternary sedi-
ments,  3,  4,  5  –  Paleogene,  6–  Mesozoic,  7–  ultramafic  body
near Sedlice. (source: http://www.geology.sk/)

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type Babington or a Burgener pumped nebulizer and a cooled
quartz glass spray chamber. The whole-rock chemical compo-
sitions are reviewed in Table 1. The rock mineral composi-
tions were calculated from the whole-rock and mineral
chemical compositions (e.g. Bodinier & Godard 2007).

The chemical compositions of mineral phases were mea-

sured by Cameca SX-100 four-spectrometer electron micro-
probe at the State Geological Institute of Dionýz Štúr in
Bratislava under the operating conditions of 15 kV accelerat-
ing voltage, 20 nA focused beam current (

φ1—5 ηm)and

Sample

SE-2

SE-14

SE-15

SE-6b

SE-12

SE-17b

Rock type

dun

harz

lherz

Ol (wt. %)

98.5

79.65

79.58

71.2

66.5

69.21

Opx (wt. %) 0

17.5

18.21

23.46

24.5

Cpx (wt. %) 0

2.5

1.85

4.69

8.33

5.53

Sp (wt. %)

1.5

0.35

0.36

0.65

0.17

0.76

Major elements (wt. %)

SiO

38.47

39.11

41.00

41.02

42.70

40.22

TiO

0.04

0.05

0.06

0.07

0.13

0.48

0.43

1.31

1.74

1.69

8.37

7.97

8.35

8.23

8.51

8.08

MnO

0.11

0.12

0.11

MgO

41.09

41.51

42.93

40.24

40.19

38.15

CaO

0.69

1.62

0.58

1.21

2.10

1.45

0.01

0.02

0.03

0.04

0.02

0.01

0.02

0.03

0.02

0.17

0.19

0.28

0.41

0.34

0.28

NiO

0.30

0.26

0.29

0.25

0.22

LOI

10.36

8.86

5.99

7.37

4.26

9.52

Total

99.79

100.22

100.07

100.29

100.35

99.88

Trace elements (ppm)

6.62

7.66

9.16

11.3

14.6

12.0

18.8

23.4

28.0

42.5

64.8

59.5

1321

1448

2030

2997

2436

2089

2626

2262

2443

2160

2091

1953

128

117

123

113

112

106

0.22

0.20

0.32

0.15

0.19

0.28

8.52

66.6

23.1

0.83

0.09

2.10

0.02

0.05

0.04

0.46

0.57

0.51

3.11*

n.m.

0.30

0.50

0.10

0.40

0.05

0.02

0.01

0.02

0.01

0.02

n.m.

0.12

0.06

0.13

0.08

0.10

0.11

11.7

1.03

4.47

1.88

16.6

2.32

0.016 0.011 0.026

b.d.l.

0.025 0.011

0.081 0.025 0.059 0.023 0.055 0.023

0.005 0.002 0.004

b.d.l.

0.006 0.002

0.017 0.002 0.009

b.d.l.

0.016 0.010

0.002

0.001

0.003

0.011

0.008

0.005

0.003

0.001

0.002

0.006

0.003

0.002

0.006

0.004

0.029

0.026

0.018

0.000

0.001

0.008

0.007

0.004

0.011

0.069

0.083

0.069

0.001

0.003

0.019

0.023

0.020

0.004

0.010

0.011

0.063

0.082

0.079

0.001

0.002

0.011

0.014

0.015

0.008

0.015

0.021

0.084

0.113

0.120

0.002

0.003

0.004

0.014

0.019

0.022

0.060

0.014

0.007

0.017

0.010

0.075

0.086

0.077

0.075

0.077

0.076

0.20

b.d.l.

0.30

0.70

0.10

0.012

0.006

0.008

0.002

0.010

0.006

0.090

0.046

0.014

0.004

0.033

0.034

Table 1: The whole-rock major and trace element compositions of dunite (dun),
lherzolites (lherz) and harzburgites (harz) from Sedlice with mineral percentual as-
semblages (in wt. %). LOI – loss on ignition, b.d.l. – below detection limit,
n.m. – not measured; Cr, Ni, Zr and Pb were measured by XRF, other trace ele-
ments by ICP-MS. * – Zr value was measured by ICP-MS.

20—100 s counting time depended upon the
analysed element. The standards used for cali-
bration were: Na on albite, Si, Ca on wollasto-
nite, K on orthoclase, Mg on forsterite, Al on
Al

, Fe on fayalite, Mn on rhodonite, metal-

lic V, Cr, and Ni, Ti on TiO

, Sr on SrTiO

Nb on LiNbO

, La on LaPO

, Ce on CePO

and Ta on LiTaO

. The mineral chemical com-

positions are reviewed in Tables 2—5.

Results

Petrography

The ultramafic body from Sedlice mainly

consists  of  harzburgites  (Fig. 2a  from  sample
SE-15;  SE-6b,  SE-14);  with  lherzolites
(Fig. 2b  from  sample  SE-17b;  SE-12)  and
dunites  (samples  SE-2,  3)  rarely  encountered.
The  intensively  brecciated  W/SW  body  mar-
gin  was  observed  (Fig. 2c).  The  fractures  of
the  brecciated  peridotite  margin  are  healed
with  secondary  magnesite  and  calcite.  The
whole body is tectonically cracked into a sys-
tem of blocks.

Microscopically, some ultramafics, exhibit-

ing  distinctly  predominant  olivine  matrix
(Fig. 2c),  could  be  termed  dunites.  Typically
mesh  textured  granular  dunite  (samples  SE-2
and SE-3, Fig. 2c) is almost exclusively com-
posed  of  slightly  serpentinized  olivine  ( ~ 98—
99 wt. %;  from  an  incipient  to  moderate
serpentinization stage) with a minimum of or-
thopyroxene grains (about 2—5 wt. %).

Harzburgites contain about 10—15 wt. % of

orthopyroxene  and  less  than  5 wt. %  of  cli-
nopyroxene  (samples  SE-14  and  SE-15).  Or-
thopyroxene  (1)  is  mostly  porphyroclastic,
often 1 to 2 mm in size, macroscopically visi-
ble. Harzburgite orthopyroxenes often show a
strong replacement by chrysotile (Fig. 2d). Or-
thopyroxene porphyroclasts contain Spl inclu-
sions (Fig. 2e,f).

Lherzolite is another rock type in the Sed-

lice peridotite (Fig. 2b). It usually has porphy-
ric  texture  and  contains  more  porphyroclastic
Cpx  (5—10 wt. %)  besides  Opx  ( ~ 25 wt. %)
(Fig. 3a,b). Enstatite, nearly colourless with a
pinkish tinge in thin sections, mainly occurs as
subhedral,  sometimes  euhedral  porphyroclas-
tic  grains  up  to  2 mm  in  size  (Opx

Fig. 3a,b) with a distinct exsolution lamellae
system of Cpx (Fig. 3c,d). Clinopyroxene,

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diopside and/or augite (Cpx

, Fig. 3b) is colourless in thin

section, sometimes slightly brownish to greenish, usually
with Opx exsolution lamellae. Aggregates of Opx

and Cpx

(Fig. 3e,f) with anhedral shape and missing exsolution
lamellae (with exception of a few grains) represent matrix
pyroxene equivalents, surrounding Opx

and Cpx

porphyro-

clasts. Pyroxene can be partly replaced by metamorphic am-
phibole—tremolite, and spinel by chromite (Fig. 2g,h). The
magmatic Spl is often reddish-brownish in thin section
(Fig. 3e,f).

On the basis of calculated “modal” mineral compositions

(Table 1),  the  studied  ultramafic  rocks  can  be  classified  as
dunites  (sample  SE-2,  3  in  Table 1  and  4  and  Fig. 4),
harzburgites  (samples  SE-6B,  14,  15  in  Table 1  and  Fig. 4)
to  lherzolites  (samples  SE-12  and  17B  in  Table 1  and
Fig. 4). The Ol-Opx-Cpx classification diagram for peridot-
ites  (Fig. 4)  with  plotted  representative  samples  from  the
Sedlice peridotite body was constructed on the basis of cal-
culated wt. % of mineral phases (Table 1).

Mineral abbreviations used in text, tables and figures

(with exception of MgChr) are after Whitney & Evans
(2010). Amp = amphibole, Cpx = clinopyroxene, Chr = chrom-

Table 2: The chemical compositions of pyroxenes from the Sedlice peridotite body.

ite, Ctl = chrysotile, Fo = forsterite, Ol = olivine, Opx = ortho-
pyroxene, Spl = spinel, Srp = serpentine group, Mag = mag-
netite, MgChr = magnesiochromite, Tr = tremolite.

Microprobe mineral composition and whole-rock chemical
data

The major element chemical compositions of minerals are

listed in Tables 2—4.

The percentages of individual components of Wo, En and Fs

in  the  Morimoto  (1988)  classification  diagram  for  Ca-Mg-Fe
pyroxenes (Quad) classifies Opx as enstatite and Cpx as dio-
pside  and  augite  (Fig. 5,  Table 2).  The  Mg#  of  pyroxenes
varies from  ~ 0.90 to 0.92 in Opx and from  ~ 0.92 to 0.95 in
Cpx (Fig. 6). Al

contents of Opx and Cpx range from 1 to

5.58 and from 0.81 to 5.45 wt. %, respectively (Fig. 6). Or-
thopyroxene and clinopyroxene in lherzolites have higher
Al

contents and lower Mg# [ = Mg/(Mg + Fe) atomic ratio]

than those in dunites and harzburgites. The Na

O content is

very low ( < 0.5 wt. %) in Cpx.

The spinel-group minerals are the major accessory miner-

als in these rocks. According to Lindsley (1991) based on the

Sample

SE-6b

SE-10

Rock type harzburgite harzburgite harzburgite harzburgite harzburgite harzburgite harzburgite lherzolite lherzolite lherzolite
Mineral

Opx

Cpx

Opx

Cpx

Opx

Cpx

Opx

Cpx

Opx

Analysis

an25

an26

an28

an27

an29

an30

an24

an8

an7

an13

(wt. %)
SiO

56.85

53.13

56.23

52.78

56.41

53.00

53.47

55.47

51.34 54.82

TiO

0.05

0.13

0.03

0.12

0.05

0.15

0.13

0.05

0.13

0.05

2.94

3.31

3.40

3.98

3.11

3.48

3.55

4.45

4.93

4.72

0.67

1.03

0.88

1.33

0.87

1.38

1.14

0.93

1.30

0.97

FeO

5.71

2.34

5.66

2.15

5.76

1.85

2.35

5.88

2.35

5.96

MnO

0.12

0.08

0.10

0.08

0.15

0.09

0.08

0.16

0.09

0.13

MgO

34.04

17.07

33.41

16.59

33.70

16.47

17.48

32.09

16.01 32.86

CaO

0.89

23.39

0.97

23.41

0.65

23.75

22.53

0.92

24.02 0.95

NiO

0.11

0.07

0.09

0.08

0.13

0.08

0.03

0.08

0.06

0.13

0.33

0.01

0.41

0.02

0.45

0.35

0.14

0.01

0.02

0.01

Total

101.38

100.87

100.78

100.96

100.85

100.70

101.12

100.03

100.38

100.63

(a.p.f.u.)
Si

1.935

1.912

1.927

1.899

1.931

1.912

1.917

1.922 1.863 1.883

0.065

0.088

0.073

0.101

0.069

0.088

0.083

0.078 0.137 0.117

0.000

0.000 0.000 0.000

2.000

2.000 2.000 2.000

0.053

0.052

0.065

0.068

0.057

0.060

0.066

0.104 0.073 0.074

0.000

0.027

0.000

0.024

0.000

0.017

0.005

0.000 0.034 0.023

0.001

0.004

0.001

0.003

0.001

0.004

0.003

0.001 0.003 0.001

0.018

0.029

0.024

0.038

0.024

0.039

0.032

0.025 0.037 0.026

0.928

0.889

0.911

0.867

0.918

0.879

0.893

0.870 0.852 0.875

0.000

0.000 0.000 0.000

0.000

0.000 0.000 0.000

1.000

1.000 1.000 1.000

0.798

0.027

0.796

0.023

0.802

0.006

0.041

0.788 0.014 0.808

0.163

0.044

0.162

0.041

0.165

0.038

0.066

0.170 0.037 0.148

0.003

0.002

0.004

0.003

0.002

0.005 0.003 0.004

0.033

0.902

0.036

0.902

0.024

0.918

0.865

0.034 0.934 0.035

0.000

0.023

0.000

0.029

0.002

0.031

0.024

0.000 0.010 0.001

0.997

0.998

0.997

0.996

0.997

0.999

0.997 0.998 0.996

1.69

45.81

1.87

46.29

1.25

47.37

43.92

1.83 46.13

1.88

89.85

51.71

89.61

51.36

90.11

50.44

52.39

89.02

51.65 90.19

8.46

2.47

8.52

2.35

8.63

2.19

3.69

9.15

2.22

7.94

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mineral chemical compositions (Table 3), they are classified
as  spinel,  magnesiochromite  and  chromite  end-members
(Fig. 7a).  The  harzburgites  contain  only  magnesiochromite
and  chromite,  whereas  lherzolites  also  preserve  the  spinel
end member. Chromite grains are round-shaped or euhedral,
sometimes  weakly  cataclastic.  They  are  accumulated  along
mineral grain boundaries, in serpentine veins in the form of
mineral  inclusions  or  dispersed  as  small  and / or  large  grain
clusters. Magnetite is the youngest of the spinel-group min-
erals. It occurs in the form of large patches around primary
reddish  spinel,  or  it  kneads  the  cataclastic  chromite  in  the
form of veins. A single grain of andradite garnet was found
in the more altered part of harzburgite.

Spinel compositions vary widely between samples. Spinel

in  harzburgites  is  represented  by  rounded,  usually  euhedral
to  subhedral  chromite  and  vermicular  magnesiochromite.  It
is  systematically  higher  in  Cr#[ = Cr/(Cr + Al)  atomic  ratio;
Cr# = 0.58—0.85] and lower in Mg#[ = Mg/(Mg + Fe

) atomic

ratio; Mg# = 0.37—0.60] than that in lherzolites, represented
by reddish spinel (Cr# = 0.14—0.37; Mg# = 0.66—0.79; Fig. 7a).
The TiO

content is low ( < 0.22 wt. %; Fig. 7b) in all cases,

only the sample SE-14 represented by harzburgite has signif-

Table 2: Continued.

icantly higher TiO

contents in the range from 0.18 to 0.21

compared to other samples. Cr# in Spl/Fo in Ol diagram
(Fig. 8a) and Cr

/Al

Spl diagram (Fig. 8b) plot most of

the samples in the Mantle-array. The only exception is sam-
ple SE-3 containing Spl with an increased Cr#, which is
compatible with the dunite as the hosting rock.

Olivine is the most representative rock-forming mineral

with forsterite content ranging from 89.0 to 91.4 in lherzolites,
and from 90.0 to 92.0 in harzburgites. The NiO content of oli-
vine ranges from 0.31 to 0.47 wt. % in harzburgites, and from
0.36  to  0.51 wt. %  in  lherzolites  (Table 4).  The  relationship
between the Fo content of olivine and Cr# of spinel shows that
all  lherzolites  and  harzburgites  plot  into  the  Ol-Spl  mantle
array  (OSMA),  a  residual  mantle  trend  of  spinel  peridotite
(Arai 1987, 1994; Fig. 8a). Olivine composition is in correla-
tion with spinel; spinel Cr# increases and spinel Mg# decreases
as olivine Fo increases in the OSMA (Choi et al. 2008).

The Primitive Mantle (PM) normalized rare earth element

concentrations from the whole-rock analyses are plotted in
Fig. 9. They show a decrease in REE as a whole, but a relative
increase in LREE, particularly Ce and La, in comparison with
HREE. Three to four samples exhibit a positive Eu anomaly.

Sample

SE-10

SE-15

Rock type lherzolite lherzolite lherzolite lherzolite harzburgite harzburgite harzburgite harzburgite harzburgite harzburgite harzburgite
Mineral

Cpx

Opx

Cpx

Opx

Cpx

Analysis

an12

an14

an15

an11

an4

an8

an21

an23

an3

an6

an16

(wt. %)
SiO

51.24 55.15 51.67 52.52 56.92

57.15

57.46

57.40

53.56

53.83

54.38

TiO

0.15 0.02 0.11 0.10 0.02

0.01

0.03

0.02

0.00

0.01

5.15 4.84 4.77 4.04 1.36

1.02

1.14

1.23

1.09

0.81

1.13

1.25 0.89 1.05 0.80 0.56

0.33

0.46

0.51

0.53

0.33

0.73

FeO

2.13 6.26 2.49 2.52 5.53

5.32

5.20

5.50

2.06

1.89

1.79

MnO

0.08 0.09 0.13 0.11 0.16

0.14

0.13

0.16

0.08

0.05

0.07

MgO

16.11 32.62 16.56 17.07 34.38

34.63

34.75

34.09

18.13

17.92

18.15

CaO

24.03 0.54 23.51 23.26 0.87

0.77

0.75

0.90

23.64

24.11

24.03

NiO

0.00 0.12 0.05 0.04 0.09

0.10

0.06

0.05

0.09

0.04

0.10 0.03 0.07 0.11 0

0.01

0.07

0.01

Total

100.24 100.57 100.42 100.58 99.89

99.46

99.99

99.89

99.22

99.12

100.40

(a.p.f.u.)
Si

1.860

1.898

1.871

1.896

1.963

1.976

1.982

1.954

1.967

1.962

0.140

0.102

0.129

0.104

0.037

0.024

0.018

0.046

0.033

0.038

0.000

2.000

0.080

0.094

0.075

0.068

0.018

0.017

0.022

0.032

0.001

0.002

0.011

0.024

0.000

0.027

0.018

0.008

0.004

0.000

0.037

0.031

0.013

0.004

0.001

0.003

0.001

0.000

0.001

0.000

0.036

0.024

0.030

0.023

0.015

0.009

0.013

0.014

0.015

0.010

0.021

0.857

0.881

0.866

0.889

0.958

0.970

0.965

0.954

0.946

0.957

0.955

0.000

1.000

0.015

0.792

0.028

0.030

0.809

0.815

0.816

0.801

0.040

0.020

0.021

0.041

0.180

0.049

0.058

0.151

0.150

0.159

0.026

0.027

0.041

0.003

0.004

0.003

0.005

0.004

0.005

0.002

0.934

0.020

0.912

0.900

0.032

0.029

0.028

0.033

0.924

0.944

0.929

0.007

0.002

0.005

0.008

0.000

0.001

0.000

0.005

1.000

0.996

0.998

0.999

0.998

0.997

0.998

0.997

0.999

46.05 1.06 44.66 44.55 1.65

1.46

1.42

1.72

45.50

46.84

46.43

51.54 89.33 52.49 52.14 90.59

90.91

90.94

90.12

53.09

51.75

51.42

2.41 9.61 2.86 3.31 7.76

7.63

7.64

8.16

1.41

2.15

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Fig. 2. a – Serpentinized harzburgite (sample SE-15) from Sedlice peridotite with preserved pyroxene porphyroclasts; b – Slightly ser-
pentinized lherzolite from Sedlice peridotite (sample SE-17b); c — Tectonic breccia composed of harzburgite angular fragments cemented
by carbonates – calcite and magnesite; d – Photomicrograph (cross-polarized light) of harzburgite (sample SE-15) with Opx

porphyro-

clasts in olivine-rich matrix; e – Photomicrograph (reflected light) of granular dunite (sample SE-3) from Sedlice locality with typical
mesh textured serpentine minerals forming veins surrounding the relic center of olivine grains; f – BSE image of serpentinized dunite
(sample SE-3) with outlined boundary of rare orthopyroxene (1); g – Photomicrograph (cross-polarized light); h – BSE image of spinel
rim dissolution-reprecipitation replacement (Putnis 2009) by metamorphic chromite in host orthopyroxene (1) porphyroclast in Sedlice ser-
pentinized harzburgite (sample SE-6b). Orthopyroxene partly replaced by metamorphic Srp and Tr.

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Table 3:

The

chemical

compositions

spinel

group

minerals

from

the

dlice

peridotite

body.

Discussion

The dunites represent the most refractory

residual  mantle  rocks  observed  in  the
Sedlice peridotite body in association with
prevailing  harzburgites  and  exclusively
with  lherzolites.  The  studied  rocks  from
this  body  are  characterized  by  a  wide
range  of  Cr#  (from  0.14  to  0.85)  in  Spl.
The  relationship  between  Cr#  of  spinel
and  Fo  of  olivine  indicates  that  studied
rocks  are  within  the  OSMA  (Arai  1987,
1994)  and  represent  residual  equivalents
of a mantle peridotite which composition-
ally reveal a wide range of melt extraction
derived by partial melting of a more fertile
mantle  peridotite  (Fig. 8a,b).  The  Fo  con-
tent  of  olivine  and  Cr#  of  spinel  do  not
change  during  subsolidus  recrystallization
(Ozawa  1988;  Arai  1994).  The  Cr#  of
spinel-group  minerals  is  progressively  in-
creasing  with  partial  melting  degree,
which, on the other hand, reduces the orig-
inal  Al  contents  in  Spl  and  Opx,  and  the
host rock (Dick & Bullen 1984; Arai 1994;
Ohara & Ishi 1998). Therefore such a wide
range of Cr# in spinel in our rocks is good
indicator of a wide range of degrees of par-
tial  melting.  Based  on  the  cited  concepts,
the  chemical  compositions  of  chromian
spinels (Cr-Spl) are plotted in various dis-
crimination  diagrams.  The  spinel  data  for
lherzolite (SE-12, SE-17b) and harzburgite
(SE-6b,  SE-14,  SE-15)  are  plotted  within
the  mantle  array  on  an  Al

/Cr

dia-

gram  (Fig. 8b).  In  the  diagram  Mg#/Cr#
(Fig. 7a) the most Cr-spinels from lherzo-
lite  (i.e.  plot  of  the  lowest  Cr#  values;
samples  SE-12  and  SE-17b)  indicate  its
relatively  undepleted  nature.  On  the  other
hand,  the  Cr-spinel  data  of  refractory
harzburgite (samples SE-14 and SE-15) in-
dicates depleted character. The highest de-
pletion of the mantle rocks is inferred in an
arc tectonic setting and/or in a supra-sub-
duction zone environment (e.g. Arai 1994;
Choi  et  al.  2008).  The  Cr#  of  spinel  in
abyssal  peridotites  collected  from  mid-
ocean  ridges  is  less  than  0.6  (Tamura  &
Arai  2006).  Our  samples  have  mostly
comparable  (SE-15,  SE-14),  but  also
slightly  higher  (SE-3)  values  (Figs. 7,  8).
The TiO

content is extremely low in arc/

back-arc  magma,  intermediate  in  mature
mid-oceanic  ridge  magma  and  high  in  in-
tra-plate  magma  (Arai  1992).  The  spinel
TiO

contents plotted in Fig. 7b record low

concentrations in all samples. The diagram
Mg# versus Al

content in pyroxenes

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Fig. 3. Photomicrographs of a slightly serpentinized Spl lherzolite (samples SE-12) from Sedlice peridotite. a – Photomicrograph (cross-po-
larized light) of porphyroclastic Opx

with Spl inclusion (in the frame); b – BSE image of Spl inclusion in Opx

(from image in a); c – Pho-

tomicrograph (cross-polarized light) of exsolved clinopyroxene lamellae in host Opx

(a BSE image detail in d frame); d – BSE image

detail of c in the frame; e – Photomicrograph (plain-polarized light) of brown-reddish spinel in Opx

—Cpx

aggregate; f – BSE image of

spinel from e.

(Fig. 6) shows differences in composition between lherzolite
and harzburgite most likely due to variable degrees of their
depletion.

Trace rare earth element concentrations from whole-rock

analyses are plotted in Fig. 9 and exhibit a depletion trend
in harzburgites, corresponding to their refractory origin in

relationship  to  more  fertile  lherzolites.  The  basic  trend  in
PM  normalized  REE  patterns  (Fig. 9a)  indicates  a  depleted
rock-suite, however an increase in LREE to HREE is similar
to  the  Dobšiná  meta-harzburgites  (Putiš  et  al.  2012),  likely
indicating an influence of metamorphic fluids during serpen-
tinization.  The  whole-rock  positive  Eu  anomaly  suggests

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Fig. 4. Classification diagram for peridotites with representative
samples from Sedlice peridotite body plotted and calculated on the
basis of primary mineral phases and whole-rock chemical composi-
tions (mineral quantities are calculated in wt. %; Table 1). The pale
green area represents the most common compositions of peridotites
in the upper part of the Earth’s mantle (partly adapted from Bodinier
& Godard (2007)).

Sample

SE-3

SE-6b

SE-14

SE-15

SE-12 SE-17b

Rock type

dun

harz

lherz

# of analyses

(wt. %)
SiO

41.37

40.98

41.61

41.38

40.98

41.38

FeO

(tot)

8.28

8.82

8.49

8.03

9.01

9.05

MnO

0.12

0.13

0.11

0.12

0.13

0.14

MgO

50.33

49.42

50.22

50.04

49.67

49.27

CaO

0.01

0.03

0.01

0.02

0.03

0.25

NiO

0.40

0.41

0.42

0.39

0.42

Total

100.56

99.87 100.92 100.06 100.33 100.60

Mg#

0.92

0.91

0.92

0.91

91.18

90.50

90.95

91.37

90.35

89.98

Table 5: The chemical compositions of metamorphic minerals from the
Sedlice peridotite body.

Table 4: Olivine chemical compositions from the Sedlice peridotite
body.

Sample

SE-3

SE-6b SE-6b SE-10 SE-6b SE-6b SE-15 SE-17b

Rock type

dun

harz

lherz

harz

lherz

Mineral

Srp

Cpx

Ana No.

(wt. %)
SiO

43.49

42.66

36.83

40.27

54.78

55.09

57.23

54.78

TiO

0.03

0.04

0.01

0.19

0.06

1.55

1.96

0.17

1.24

0.92

1.22

3.92

0.01

0.64

0.83

0.00

0.35

0.27

0.50

0.77

FeO

1.63

3.20

6.35

6.66

2.01

1.57

1.95

2.18

MnO

0.03

0.08

0.19

0.25

0.12

0.13

0.04

MgO

42.35

37.89

36.23

35.90

21.29

20.38

23.29

21.90

CaO

0.02

0.11

0.06

0.23

19.08

22.12

13.50

13.28

NiO

0.16

0.02

0.10

0.36

0.02

0.15

0.11

0.08

0.09

0.01

0.55

0.30

0.13

0.64

0.02

0.06

0.02

0.04

0.18

0.11

0.01

0.03

0.05

0.46

0.13

0.04

0.05

Total

87.80

86.36

83.06

84.01

99.64 101.07

98.04

97.85

substitution of Eu

for Ca

, likely in tremolite (in the B site)

or rare carbonates. The trace element mobility is also docu-
mented in spider diagram (Fig. 9b) showing a relative increase
in Cs, Ba, U, Ta, Ce, Sr, Zr, Hf and Ti. The main difference
between the less and more depleted rocks exhibit HREE and
Ti, which are increased in (less depleted) lherzolites.

From this point of view, the harzburgites from the Sedlice

peridotite  body  could  be  genetically  bound  to  an  abyssal
mantle  peridotite  (e.g.  Bodinier  &  Godard  2007).  Some  of
the  Spl  analyses  at  the  boundary  of  the  mantle  array  could
indicate either a higher melting degree, or a later influence of
metamorphic fluids, or both.

The studied peridotite body exhibits features of low-temper-

ature metamorphic overprint. Metamorphic mineral assem-

Fig. 5. Pyroxenes from Sedlice peridotite in the Morimoto (1988)
classification.

blage contains chrysotile, tremolite, andradite garnet,
Cr-spinel  to  chromite  and  magnetite,  an  increase  of
fayalite  component  in  olivine,  and  rare  carbonate.
This might be related to serpentinization and a weak
rodingitization in an accretionary wedge, resembling
the Meliatic Bôrka Nappe serpentinized and rodingi-
tized harzburgites (Putiš et al. 2012; Li et al. 2014).
Because  of  practically  missing  high-pressure  meta-
morphic  overprint,  characteristic  for  the  Meliatic
Bôrka  blueschist-bearing  nappe  (with  antigorite-
clinopyroxene-pargasite-bearing  meta-harzburgites,
Putiš  et  al.  2012),  this  body  could  indicate  an  ob-
duction process and incorporation into an accretion-
ary wedge due to closure of the Neotethyan Meliatic
(Triassic—Jurassic) oceanic back-arc basin in the Late
Jurassic  (Dallmeyer  et  al.  1996;  Mock  et  al.  1998;
Faryad et al. 2005; Putiš et al. 2011).

The Sedlice body could be an olistolith, which

slided into the Paleogene sediments from the Bôrka
Nappe, overlying the Central Western Carpathians

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orogenic  wedge  since  the  Late  Cretaceous.  Alternatively  it
could be a younger tectonic protrusion body from the under-
lying  basement  units,  most  likely  from  the  Meliatic  Bôrka
Nappe,  which  originated  after  covering  by  the  Paleogene
basal  and  younger  flysch  sediments.  Nevertheless,  the  sur-
face occurrences of the metaperidotites of the Bôrka Nappe
are not so far away – along the Gemeric/Veporic Late Cre-
taceous tectonic boundary, to the south (SW) of the Central-
Carpathian Paleogene Basin (Fig. 1). The brecciation of the
body margin healed by magnesite and calcite postdates per-
vasive  and  relatively  higher-temperature  serpentinization
most likely in an accretionary wedge. Therefore the breccia-
tion might reflect an interaction of CO

-rich water with the

body margin within the sedimentary basin.

Conclusions

The spinel peridotite from Sedlice comprises mainly depleted

harzburgites accompanied by lherzolites and dunites, which

Fig. 6. Plot of Mg#[ = Mg/(Mg + Fe) atomic ratio] versus Al

con-

tents (wt. %) in monoclinic and rhombic pyroxenes from Sedlice
peridotite.

Fig. 7. Spinel compositional variations in the peridotite body from
Sedlice. a – Relationship between Cr#[ = Cr/(Cr + Al) atomic ratio]
and TiO

content; b – Relationship between Mg#[ = Mg/(Mg + Fe

)

atomic ratio] and Cr#. The individual spinel-group end-member
mineral terminology is after Lindsley (1991).

formed in a spinel stability field mantle environment. The stud-
ied samples point to a wide range of depletion. By composition,
the lherzolites are close to fertile spinel lherzolites. The
harzburgites represent depleted mantle rocks or residual equi-
valents formed by various degree of partial melting of more
fertile lherzolites. The depletion is recorded in their refractory
lithology and mineral chemical compositions. Cumulates, the
expected derivatives formed by magmatic differentiation or a
higher degree partial melting were not found in this body.

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Fig. 9. a – Primitive Man; b– Spider diagram from
Sedlice peridotite.

Fig. 8.  a  –  Compositional  relationship  between  Fo[ = Mg/
((Mg + Fe + Ca + Ni)/100)  atomic  ratio]  content  of  olivine  and
Cr#[ = Cr/(Cr+Al) atomic ratio] of spinel from the Sedlice peridotite
body.  OSMA  (Olivine—Spinel  Mantle  Array)  is  a  spinel  peridotite
residual trend and with melting trend (red curved line annotated by
melting  %)  are  from  Arai  (1987,  1994).  FMM  –  fertile  MORB
mantle;  b  –  Discrimination  diagram  Al

versus Cr

(wt. %)

with plotted spinels from the Sedlice peridotite body (after Franz &
Wirth 2000).

The PM normalized REE patterns indicate a de-

pleted rock-suite, however an increase in LREE to
HREE most likely reveals an influence of meta-
morphic fluids due to serpentinization. The
whole-rock positive Eu anomaly might have been
caused by substitution of Eu

for Ca

in tremo-

lite or rare carbonates.

The low-temperature metamorphic mineral as-

semblage  of  peridotite  body  contains  chrysotile,
tremolite,  rare  andradite  garnet,  Cr-spinel  to
chromite  and  magnetite,  and  rare  carbonate;  this
could  also  be  determined  by  an  increase  of  the
fayalite  component  in  olivine.  These  features  re-
semble  the  Meliatic  meta-harzburgites  in  the
Western Carpathians.

The Sedlice peridotite body most likely formed

from  the  Meliatic  Bôrka  Nappe  slices  and  cur-
rently  appears  to  be  a  protrusive(?)  body  within
the  Central-Carpathian  Paleogene  sediments.  The
brittle  fractures  healed  by  magnesite  and  calcite
crosscut  the  serpentinized  peridotite  body  and

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therefore may represent a younger carbonate mineralization
of unclear age.

Acknowledgments: This work was supported by the APVV-
0081-10  and  VEGA-1/0255/11  scientific  Grants  (M.P.).
Doc.  RNDr.  Pavel  Fejdi,  CSc.  deserves  special  thanks  for
grateful suggestions and helpful experiences. We honour his
memory. The suggestions of J. Ulrych, D. Hovorka and one
anonymous  reviewer  are  greatly  acknowledged.  We  also
thank M. Styan for reviewing the English content.

References

Arai S. 1987: An estimation of the least depleted spinel peridotite

on the basis of olivine—spinel mantle array. Neu. Jb. Miner.
Monat. 8, 347—354.

Arai S. 1994: Characterization of spinel peridotites by olivine—

spinel compositional relationships: review and interpretation.
Chem. Geol. 113, 191—204.

Biely A., Bezák V., Elečko M., Gross P., Kaličiak M., Konečný V.,

Lexa J., Mello J., Nemčok J., Potfaj M., Rakús M., Vass D.,
Vozár J. & Vozárová A. 1996: Geological map of Slovakia,
1 : 500,000. State Geological Institute of Dionýz Štúr Publishers,
Bratislava.

Bodinier J.L. & Godard M. 2007: Orogenic, ophiolitic, and abyssal

peridotites. In: Carlson R.W. (Ed.): Treatise on geochemistry.
Vol. 2. Elsevier, Amsterdam, 1—73.

Brandon M.T. 2004: The Cascadia subduction wedge: the role of ac-

cretion, uplift, and erosion. In: van der Pluijm B.A. & Marshak
S. (Eds.): Earth structure: An introduction to structural geology
and tectonics. 2nd ed. WCB/McGraw Hill Press, 566—574.

Burnham M., Meisel T. & Kriete C. 2010: OKUM and MUH-1: two

new IAG-certified ultramafic rock reference materials.
Geochim. Cosmochim. Acta 74, Suppl 1, A129.

Cambel B. 1951: Ultrabasic rock from Sedlice and serpentines of

the closest surrounding. [Ultrabázická hornina od Sedlíc
a hadce najbližšieho okolia.] Geol. Zbor. Slovak. Akad. Vied 2,
1—91 (in Slovak).

Choi S.H., Shervais J.W. & Mukasa S.B. 2008: Supra-subduction

and abyssal mantle peridotites of the Coast Range ophiolite,
California. Contr. Mineral. Petrology 156, 551—576.

Dallmeyer R.D., Neubauer F., Handler R., Fritz H., Müller W.,

Pana D. & Putiš M. 1996: Tectonothermal evolution of the in-
ternal Alps and Carpathians: Evidence from

Ar/

Ar mineral

and whole-rock data. Eclogae Geol. Helv. 89, 203—227.

Dick H.J.B. & Bullen T. 1984: Chromian spinal as a petrogenetic

indicator in abyssal and alpine-type peridotites and spatially
associated lavas. Contr. Mineral. Petrology 86, 54—76.

Faryad S.W., Spišiak J., Horváth P., Hovorka D., Dianiška I. & Jósza

S. 2005: Petrological and geochemical features of the Meliata
mafic rocks from the sutured Triassic oceanic basin, Western
Carpathians. Ofioliti 30, 27—35.

Fejdi P. & Kolník B. 1988: Pyroxene geothermometry and geobaro-

metry of ultrabasic body near Sedlice, Eastern Slovakia. [Py-
roxénová geotermometria geobarometria ultrabázického telesa
pri Sedliciach.] Miner. Slovaca 20, 149—159 (in Slovak).

Franz L. & Wirth R. 2000: Spinel inclusions in olivine of peridotite

xenoliths from TUBAF seamount (Bismark Archipelago/Papua
New Guinea): evidence for the thermal and tectonic evolution of
the oceanic lithosphere. Contr. Mineral. Petrology 140, 283—295.

Gnojek P. & Kubeš P. 1991: Magnetometric evidence to the Sedlice

ultramafic body. [Svědectví magnetometrie o ultrabázickém
tělese u Sedlíc.] Miner. Slovaca 23, 161—164 (in Czech).

Hovorka D. 1977: Geochemistry of the West Carpathian Alpine-

type ultramafites. Veda, Nauka o Zemi, Geol. 12, 1—148.

Hovorka D., Dubíková K., Gerthoferová H., Šamajová E. & Turan

J. 1980: Serpentine – group minerals of the Western Car-
pathians ultramafics. I. Bodies of the Gemeride Mesozoic.
Miner. Slovaca 12, 481—506.

Hovorka D., Ivan P., Jaroš J., Kratochvíl M., Reichwalder P., Roj-

kovič I., Spišiak J. & Turanová L. 1985: Ultramafic rocks of
the Western Carpathians. GÚDŠ, Bratislava, 1—253.

Jaroš J., Kratochvíl M. & Zlocha J. 1981: Mesoscopic structural

analysis of serpentinite bodies in the Spišsko-gemerské ru-
dohorie Mts. (Eastern Slovakia). [Drobnoštruktúrna analýza
vnútornej stavby serpentinitových telies v Spišsko-gemerskom
rudohorí.] Miner. Slovaca 13, 527—548 (in Slovak).

Kantor J. 1955: Ore minerals of Spiš-Gemeric serpentinites

(awaruite, heazlewoodite etc.). [Rudné minerály Spišsko-Ge-
merských serpentinitov (awaruit, heazlewoodit at .).] Geol.
Zbor. Slov. Akad. Vied 6, 1—302 (in Slovak).

Li X.-H., Putiš M., Yang Y.-H., Koppa M. & Dyda M. 2014: Accre-

tionary wedge harzburgite serpentinization and rodingitization
constrained by perovskite U/Pb SIMS age, trace elements and
Sm/Nd isotopes: case study from the Western Carpathians,
Slovakia. Lithos 205, 1—14.

Lindsley D.H. 1991: Oxide minerals: petrologic and magnetic sig-

nificance. Rev. in Mineralogy 25, 1—509.

Marschalko R. 1966: Geology and sedimentology of marginal flysch

lithophacies from the central Carpathians (Šariš highlands).
[Geológia a sedimentológia flyšových okrajových litofácií cen-
trálnych Karpát (Šarišská hornatina).] Sbor. Geol. Vied, Zá-
pad. Karpaty 5, 1—9 (in Slovak).

McDonough W.F. & Sun S. 1995: The composition of the Earth.

Chem. Geol. 120, 223—253.

Meisel T., Schöner N., Paliulionyte V. & Kahr E. 2002: Determina-

tion of rare earth elements (REE), Y, Th, Zr, Hf, Nb and Ta in
geological reference materials G-2, G-3, SCo-1 and WGB-1 by
sodium peroxide sintering and ICP-MS. Geostand. Newsl. 26,
53—61.

Mikuš T. & Spišiak J. 2007: Chemical composition and alter ation

of Cr-spinels from Meliata and Penninic serpentinized peridot-
ites (Western Carpathians and Eastern Alps). Geologica Q. 51,
257—270.

Mock R., Sýkora M., Aubrecht R., Ožvoldová L., Kronome B.,

Reichwalder P. & Jablonský J. 1998: Petrology and petrography
of the Meliaticum near the Meliata and Jaklovce villages, Slo-
vakia. Slovak Geol. Mag. 4, 223—260.

Morimoto N., Fabries J., Ferguson A.K., Ginzburg I.V., Ross M.,

Seifert F.A. & Zussman J. 1988: Nomenclature of pyroxenes.
Amer. Mineral. 73, 1123—1133.

Plašienka D., Grecula P., Putiš M., Kováč M. & Hovorka D. 1997:

Evolution and structure of the Western Carpathians: an over-
view. In: Grecula P., Hovorka D. & Putiš M. (Eds.): Geologi-
cal evolution of the Western Carpathians. Miner. Slovaca,
Geocomplex, Bratislava, 1—24i.

Putiš M., Koppa M., Snárska B., Koller F. & Uher P. 2012: The

blueschist-associated perovskite—andradite-bearing serpenti-
nized harzburgite from Dobšiná (the Meliata Unit), Slovakia.
J. Geosci. 58, 221—240.

Putiš M., Radvanec M., Sergeev S., Koller F., Michálek M., Snárska

B.,  Koppa  M.,  Šarinová  K.  &  Németh  Z.  2011:  Metamor-
phosed succession of cherty shales with basalt and diastrophic
breccia  in  olistolith  of  the  Meliatic  Jurassic  accretion  wedge
near  Jaklovce  (Slovakia),  dated  on  zircon  (U—Pb  SIMS
SHRIMP). Miner. Slovaca 43, 1—18.

Putnis A. 2009: Mineral replacement reactions. Rev. Mineral.

Geochem. 70, 87—124.

Radvanec M. 2000: P-T path and exhumation of ultra-high pressure

399

PERIDOTITE BODY IN CENTRAL CARPATHIAN PALEOGENE SEDIMENTS (E SLOVAKIA)

GEOL

EOL

EOLOGICA CARPA

OGICA CARPA

OGICA CARPATHICA

THICA

THICA, 2014, 65, 4, 387—399

metamorphosed  peridotite  at  Jaklovce  on  the  north  of  Gemeri-
cum and on the locality Skalka at Sedlice northward of the zone
Branisko—Čierna  hora  Mts.  (Western  Carpathians,  Slovakia).
[P-T  dráha  exhumácie  ultravysokotlakovo  metamorfovaného
peridotite  ne aleko  Jakloviec  na  severe  gemerika  a  na  lokalite
Skalka pri Sedliciach na sever od pruhu Branisko—Čierna hora.]
Miner. Slovaca 32, 439—458 (in Slovak).

Rojkovič I. 1985: Ore mineralization of ultramafic bodies in West-

ern Carpathians. [Rudná mineralizácia ultramafických telies
Západných Karpát.] Veda, SAV, Bratislava, 1—63 (in Slovak).

Rojkovič I. & Boronichin V.A. 1982: Sulphidic nickel-cobalt-iron

ores in ultramafic rocks of the Western Carpathians. [Sulfi-
dická Ni-Co-Fe mineralizácia v ultramafických horninách Zá-
padných Karpát.] Miner. Slovaca 14, 41—59 (in Slovak).

Rojkovič I. & Hovorka D. 1979: Relation of ore mineralization to

geochemistry of the West Carpathian ultramafic massifs. Geol.
Zbor. Geol. Carpath. 30, 449—462.

Rojkovič I., Hovorka D. & Krištín J. 1978: Spinel group minerals

in the West Carpathians ultrabasic rocks. Geol. Zbor. Geol.
Carpath. 29, 1—253.

Scambelluri M., Fiebig J., Malaspina N., Müntener O. & Pettke T.

2004: Serpentinite subduction: implications for fluid processes
and trace-element recycling. Int. Geol. Rev. 46, 595—613.

Stankovič J., Kadlečíková M. & Breza J. 2007: Clinopyroxene ex-

solutions  preserved  in  orthopyroxene  from  metaultramafic
rock  near  Sedlice  (Western  Carpathians)  and  their  identifica-
tion  by  Raman  Spectroscopy.  [Zachovalé  exsolúcie  klinopy-
roxénu  v  orthopyroxéne  z  metaultramafickej  horniny  pri
Sedliciach  (Západné  Karpaty)  a  ich  identifikácia  ramanovou
spektroskopiou.] Acta Geol. Univ. Comen. 1, 55—59 (in Slovak).

Tamura A. & Arai S. 2006: Harzburgite- dunite-orthopyroxenite

suite as a record of supra-subduction zone setting for the Oman
ophiolite mantle. Lithos 90, 43—56.

Whitney D.L. & Evans B.W. 2010: Abbreviations for names of

rock-forming minerals. Amer. Mineralogist 95, 185—187.

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