GeolCarp_Vol66_No5_347

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, OCTOBER 2015, 66, 5, 347—360 doi: 10.1515/geoca-2015-0030

Geochemistry of amphibolites and related graphitic gneisses

from the Suchý and Malá Magura Mountains (central

Western Carpathians) – evidence for relics of the Variscan

ophiolite complex

PETER IVAN and ŠTEFAN MÉRES

Comenius University, Faculty of Sciences, Department of Geochemistry, Ilkovičova 6G, 842 15 Bratislava, Slovak Republic;

ivan@fns.uniba.sk; meres@fns.uniba.sk

(Manuscript received January 12, 2015; accepted in revised form June 23, 2015)

Abstract: Three small bodies of amphibolites and associated graphitic gneisses from the Suchý and Malá Magura
Mountains (Tatric Megaunit, central Western Carpathians) have been studied by petrographic and geochemical methods.
Isolated, fault-bounded bodies first hundreds of meters in size are located in the complex of the Early Paleozoic
paragneisses and migmatites intruded by the Lower Carboniferous granitoid rocks. Amphibolites (locally actinolite
schists) were formed from effusive basalts, dolerites or isotropic gabbros hydrothermally altered and veined before the
regional metamorphic transformation. Distribution of the trace elements relatively immobile during the metamorphic
alteration (HFSE, REE, Cr, V, Sc) is similar to E-MORB type in the Malá Magura Mountain or to N-MORB/E-MORB
types in the Suchý Mountain. Graphitic gneisses to metacherts are rich in silica (up to 88 wt. %) and C

tot

, poor in other

major element contents and display negative Ce-anomaly, enrichment in HREE, V, Cr and U. They were probably
originally deposited as non-carbonate and silica-rich deep-sea sediments in anoxic conditions. The oceanic provenance
of amphibolites and related graphitic gneisses clearly indicates their oceanic crust affinity and identity with the upper-
most part of the ophiolite sequence. Ophiolite bodies from the Suchý and Malá Magura Mountains are supposed to be
relic fault blocks identical with the Upper Devonian Pernek Group which represents a Variscan ophiolite nappe pre-
served to large extent in the Malé Karpaty Mountains located in the Tatric Megaunit further to the southwest. All these
ophiolite relics are vestiges of the original ophiolite suture created by oceanic closure in the Lower Carboniferous.

Key words: Western Carpathians, Variscides, Suchý and Malá Magura Mts, ophiolites, metabasites, graphitic gneisses,
geochemistry.

Introduction

Ophiolite sutures, thin belts with specific rock associations,
are relics of the oceanic crust displaced into continental crust
as a result of the closure of former oceanic basins. In orogenic
belts  they  represent  fossil  boundaries  between  lithospheric
paleoplates. They are thus very important for the reconstruc-
tion  of  the  geological  history  of  orogens  (e.g.  Dilek  2003;
Dilek & Furnes 2011, 2014; Nicolas 2012). Because the ma-
jority of orogenic belts are formed as a consequence of mul-
tiple  collisions,  several  generations  of  ophiolite  sutures  can
occur (Ollier & Pain 2000; Frisch et al. 2011). Identification
of older sutures is, as a rule, very problematic due to tectonic
splitting,  thinning  and  dismembering  of  former  ophiolite
nappes in the course of their reworking by younger orogenic
activities (e.g. Zhang et al. 2008). In the following paper we
would like to show that even relatively small relics of an an-
cient  high-grade  metamorphosed  oceanic  crust  can  be  reli-
ably  identified  by  geochemical  methods  if  metamorphic
equivalents  of  basalts  together  with  related  deep-sea  sedi-
ments are still preserved. We demonstrate such identification
using  an  example  of  amphibolites  associated  with  graphitic
gneisses from the Suchý and Malá Magura Mts in the West-
ern Carpathians.

Geology

The Suchý and Malá Magura Mts (SE part of the Strážovské

vrchy  Mts)  belong  to  the  so  called  core  mountains  in  the
Tatric megaunit of the central Western Carpathians (Plašienka
et al. 1997). An Early Paleozoic crystalline core and Late Pa-
leozoic—Mesozoic cover form these mountains (Maheq 1985).
The crystalline core of the Suchý and Malá Magura Mountains
is formed by two structural parts (the western part – Suchý
core, the eastern part – Malá Magura core) separated by the
N-S trending Diviaky fault but both parts contain genetically
identical  rock  complexes  (Fig. 1).  Several  typical  features
characterize  the  geological  structure  of  this  crystalline  core:
(1)  alternation  of  paragneiss,  migmatite  and  granitoid  belts,
(2) petrographic variability of granitoids together with wide-
spread aplite-pegmatite granites and plenty of aplite and peg-
matite veins and (3) the absence of retrogression and Alpine
schistosity (Kahan 1979; Maheq 1986 and references herein).
Granitoid rocks display S-type signature (Petrík et al. 1994)
and similarly to other such granitoids in the central Western
Carpathians are of lowermost Carboniferous age (356 ± 9 Ma,
Kráq et al. 1997, U-Pb zircon evaporation technique). Meta-
morphic  rocks  are  products  of  the  progressive  Variscan
metamorphism  (Korikovsky  et  al.  1987).  Two  stages  of  the

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pre-Alpine  metamorphic  evolution  were  described  in  the
study  area  (Méres  &  Hovorka  1989;  Vilinovičová  1990;
Hovorka & Méres 1991), the former one was probably caused
by heat related to the granitoid magmatic activity and their in-
tensity decrease to the west. According to Čík & Petrík (2014)
peak  metamorphic  conditions  reached  T = 670—765 °C,  and
P ~ 600—820 MPa. Besides widespread paragneisses and their
migmatitized analogues, quartzose biotite gneisses to biotite
quartzites are also comprised in the Suchý and Malá Magura
crystalline complexes occasionally also with intensive pyrite
impregnation  and  graphitic  paragneisses  (Kahan  1980).
Metabasic  rocks  (amphibolites)  are  scarce  and  mostly  form
small bodies (first several meters) embedded in all main rock
types (cf. geological map 1 : 50,000 – Maheq et al. 1982). In
addition they also occur in granitoid rocks usually accompa-
nied by gneiss relics. Our study has been focused especially
on  the  three  largest  metabasic  bodies:  (1)  the  body  near
Nevidzany  village  in  the  valley  of  the  Krstenica  brook
(Suchý Mts), (2) the body in the Železná dolina valley N of
the village of Závada pod Čiernym vrchom (Suchý Mts) and
(3) the body near Chvojnica village, the largest of three, about
1500 m  long  and  500 m  wide  (Fig. 1).  Boundaries  between
these  bodies  and  the  surrounding  gneisses  and  migmatites
are  formed  by  faults  and  frequently  injected  by  veins  of
pegmatitoid granites, pegmatites and aplites. Metamorphosed
veinlets  with  sulphide  mineralization  and  local  sulphide  im-
pregnation  are  typical.  With  the  exception  of  the  body  near
Nevidzany  village  the  metabasite  bodies  closely  associate

with metamorphosed carbonaceous pelitic and silicic rocks
interlaid by thin laminas of sulphide ore. The direct spatial re-
lationship of the metabasic rocks with the above mentioned
rocks and sulphide mineralization is illustrated by a schematic
profile across the Chvojnica metabasite body (Fig. 2).

Petrography

Metamorphosed basic rocks from the Suchý and Malá

Magura  Mts  crystalline  complexes  have  generally  been  de-
scribed  as  typical  plagioclase  amphibolites  without  any  pe-
culiar  petrographic  features.  However,  our  detailed  study
indicates that several petrographic types could be discerned
here. The variability in such types is partly observable mac-
roscopically  as  differences  in  grain  size  mostly  inherited
from magmatic protolith or the intensity of pre-metamorphic
pervasive  seafloor  hydrothermal  alteration.  Microscopically
the  metabasites  are  composed  mostly  of  aggregates  of  am-
phibole  and  plagioclase  grains.  Ilmenite,  titanite  and  occa-
sionally biotite, clinozoisite and sulphides are also present in
subordinate  amounts.  Diopside  in  association  with  albite,
quartz and sulphides are components of metamorphosed hy-
drothermal veins. Scarce young veinlets contain prehnite and
smectite. Metabasites from the Suchý and Malá Magura Mts
could be classified into two groups based on mineral associa-
tion as well as amphibole compositions: (1) actinolite schists
(transitional  rock  type  between  greenschists  and  amphibo-

Fig. 1. Geological sketch-map of the crystalline complexes of the Suchý and Malá Magura Mts. After Maheq et al. (1982) – modified.
MK – Malé Karpaty Mts, PI – Považský Inovec Mts, SMM – Suchý and Malá Magura Mts. 1—3 – studied amphibolite bodies
(1 – Nevidzany, 2 – Železná dolina valley, 3 – Chvojnica). full star – location of the Pernek and Pezinok Grps., empty stars – loca-
tions of the Zlatník and Ochtiná Grps. (see discussion).

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lites) and (2) amphibolites. The samples with still discernible
magmatic  protolith  are  of  four  types:  (1) metabasalts,
(2) metadolerites,  (3) metagabbros  and  (4) strongly  veined
and hydrothermally altered basaltic rocks. Metabasalts were
originally  the  most  widespread  rock  type  at  both  most  sig-
nificant localities – Železná dolina valley (Suchý Mts) and
Chvojnica village (Malá Magura Mts). The former locality is
mostly  represented  by  actinolite  schists  composed  of  ori-
ented aggregate of acicular pale green to green actinolite and
plagioclase  with  subordinate  amount  of  ore  minerals  and
small  titanite  grains.  The  composition  of  plagioclase  varies
in a wide range (An

—An

). Rarely preserved phantom tex-

tural  relics  point  to  effusive  fine-grained  to  glassy  basalts
with  hyaloporphyric  and/or  intersertal  textures  (Fig. 3A,B),
massive basalts likely with ophitic texture were also present.
Some clinozoisite and diopside together with pyrite are con-
centrated  in  albite  veins.  At  the  Chvojnica  locality  basalts
were  transformed  to  amphibolites  composed  of  fine-grained
mosaic  aggregate  of  anhedral  or  subhedral  brown  amphibole
(magnesiohornblende)  and  plagioclase  (ca. An

). Impregna-

tion by ore minerals (predominantly pyrite) of variable inten-
sity is common as well as veining by network of mostly albitic
veins  also  containing  diopside,  amphibole  and  ore  minerals.
Some  metabasites,  originally  intensively  hydrothermally  al-
tered,  comprise  diopside  not  only  in  veins,  but  also  in  sur-
rounding rock with decreasing quantity away from the veins.

Metadolerites display still preserved indices of ophitic/

doleritic  texture  in  the  form  of  alternation  of  almost  mono-
mineralic sub-aggregates of brown amphibole with sub-aggre-
gates  of  the  mosaic  plagioclase  including  small  amounts  of
fine  amphibole  crystals  and  following  orientations  of  the
original  magmatic  plagioclase  laths  (Fig. 3C).  Metadolerites
have  been  identified  at  localities  Železná  dolina  valley  (in  a
small isolated body) and Chvojnica village.

Amphibolites formed from the flaser gabbro protolith

could be revealed based on the specific texture represented

by  alternation  of  attenuated  lenses  composed  of  the  brown
amphibole  monomineralic  aggregate  with  lenses  of  mosaic
amphibole-plagioclase  aggregates  displaying  variable  ratio
of both minerals. Rare lens-shaped clusters of titanite/ilmenite
grains, sporadic crystals of dark mica and impregnation with
sulphides are also present. Metagabbros form the body near
Nevidzany village (Suchý Mts) and rarely occur in the body
near Chvojnica village (Malá Magura Mts), where types with
relic granular texture have also been found (Fig. 3F).

Metamorphosed carbonaceous sedimentary rocks closely

spatially related to metabasic rocks are generally present as
graphitic gneisses. They macroscopically form dark grey to
black rocks, mostly siliceous, with schistose structure locally
intercalated by light grey belts with intensive sulphide im-
pregnations.

Microscopically the lepidogranoblastic and granoblastic

textures are dominant (Fig. 3E,F). Plagioclase, white micas,
metamorphosed organic matter and quartz, are common min-
eral  components,  while  tourmaline,  garnet,  sillimanite  and
ore minerals are relatively rare. Vanadium-rich aluminosili-
cates, such as goldmanite (Bačík et al. 2012), V-rich tourma-
line (Bačík et al. 2011) and V-rich mica – roscoelite (Méres
& Ivan 2007) have also been found in these rocks. They were
locally formed in the course of regional metamorphism from
the  originally  vanadium-rich  protolith  represented  by  sedi-
ment  rich  in  organic  matter.  Metacherts  are  compositionally
similar  to  graphitic  gneisses  only  with  comparatively  high
content of quartz and lower content of plagioclase. Layers of
quartz-sericite phyllites with variable content of tremolite/ac-
tinolite, carbonaceous matter and sulphides are also present in
this sequence of the metamorphosed sedimentary rocks.

All the types of metamorphosed basic and carbonaceous

sedimentary rocks identified in the Suchý and Malá Magura
Mts are petrographically very similar to those from the Pernek
Group in the Malé Karpaty Mts (cf. Ivan et al. 2001; Méres
2005; Ivan 2009).

Fig. 2. A – Geological sketch-map of the amphibolite body near Chvojnica village with location of the geological profile depicted in
Fig. 2B. Modified after Maheq et al. (1982); B – Schematic geological profile across zone of the metamorphosed sedimentary rocks with
sulphide mineralization located in the amphibolite body near the Chvojnica village (Malá Magura Mts). Profile follows morphological
ridge between the NW border and central part of the NW-SE oriented amphibolite body.

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Analytical methods

The chemical composition of the rocks was determined at

the ACME Analytical Laboratories (Vancouver, Canada).

Total abundances of major element oxides were deter-

mined  by  inductively  coupled  plasma  –  emission  spectro-
metry  (ICP-ES)  following  lithium  metaborate-tetraborate
fusion  and  dilute  nitric  acid  treatment.  Loss  on  ignition
(LOI) was calculated from the difference in weight after ig-
nition to 1000 °C. For the total carbon (TOT/C) and sulphur
analysis  (TOT/S)  by  LECO  analysis,  the  samples  were
heated  in  an  induction  furnace  to  > 1650 °C  which  caused
the  volatilization  of  all  C  and  S  bearing  phases.  Vapours
were carried through an infrared spectrometric cell wherein
the  concentrations  of  C  and  S  were  determined  by  the  ab-
sorption  of  specific  wavelengths  in  the  infrared  spectra
(ORG/C = TOT/C minus graphite C and carbonate). Concen-
trations of trace elements and rare earth elements were deter-
mined by ICP mass spectrometry (ICP-MS). Further details

are accessible on the web page of the ACME Analytical
Laboratories (http://acmelab.com/).

Geochemistry

Major and trace elements distribution in selected samples

of metabasic rocks from the Suchý and Malá Magura Mts is
demonstrated in Table 1.

Major element concentrations in the studied rocks fully re-

flect their basic basaltic character. The basaltic composition
of these rocks is also supported by their position in diagrams
Zr/TiO

vs. SiO

(Winchester & Floyd 1977) or Nb/Y vs. Zr/Ti

(Pearce  1996;  Fig. 4),  falling  into  the  field  of  non-alkaline
basalts.  Their  tholeiitic  character  is  revealed  by  a  Zr/Y  vs.
Th/Yb  discrimination  diagram  (Ross  &  Bédard  2009).  Com-
positions  mostly  compatible  with  primary  basaltic  liquids,
less frequently also with more differentiated Fe-Ti basalts, are
indicated  by  TiO

vs. Al

diagram (Pearce 1983; Fig. 5).

Table 1: Major and trace element analyses of the metamorphosed basic rocks from the Suchý and Malá Magura Mts. Note: Samples la-
belled AMM – Malá Magura Mts, ASU – Suchý Mts. Location and GPS coordinates of samples – see appendix.

AMM- ASU-

Sample

15A

1 5 6 7 8 12

SiO

46.71 48.20 49.59 49.39 49.00 46.13 46.20 48.65 48.80 48.50 48.53 46.72

TiO

1.72 1.84 2.12 1.84 1.89 1.53 1.87 1.18 1.35 2.26 2.23 2.55

14.23 16.01 16.75 15.11 15.23 14.22 14.37 14.29 16.13 15.78 15.64 15.75

3tot

12.02 10.84 9.18 10.77 11.05 10.44 12.12 10.27 10.36 10.90 10.28 11.34

MnO

0.13 0.12 0.11 0.15 0.14 0.15 0.13 0.17 0.16 0.18 0.13 0.15

MgO

8.68 5.73 5.51 7.24 7.55 12.72 8.54 8.62 6.72 7.70 6.72 6.26

CaO

11.25 12.49 11.94 10.36 10.49 10.05 12.24 11.10 10.65 9.11 10.37 11.91

2.75 3.30 3.28 2.97 2.99 2.42 1.70 2.85 3.09 3.71 4.07 2.98

0.55 0.29 0.18 0.44 0.31 0.18 0.55 0.44 0.87 0.15 0.12 0.28

0.17 0.18 0.20 0.18 0.17 0.15 0.20 0.07 0.18 0.22 0.23 0.31

LOI

1.40 0.70 0.80 1.20 0.80 1.60 1.60 2.00 1.40 1.20 1.30 1.40

tot

<0.02 0.02 0.04 0.03 0.04 0.03 0.03 0.04 0.07 0.03 <0.02 <0.02

tot

<0.02 0.11 <0.02 0.03 <0.02 <0.02 0.05 <0.02 <0.02 <0.02 0.76 0.04

Total

99.72 99.77 99.75 99.68 99.67 99.67 99.69 99.73 99.77 99.72 99.73 99.73

108

112

140

115

127

136

73.8

65.5

155

154

186

28.3

29.3

30.9

30.5

23.3

20.6

28.2

34.5

33.6

40.8

3.2

3.9

3.4

3.3

2.7

3.6

1.9

4.5

4.9

0.7

0.8

0.7

0.6

0.7

<0.2

0.5

0.2

<0.2

0.3

2.3

0.2

0.1

0.7

0.1

0.9

0.1

0.2

0.8

0.5

0.6

0.5

0.2

0.4

0.1

<0.1

0.4

0.3

0.6

7.9

8.1

9.8

9.5

2.1

6.2

2.1

0.4

7.4

479

335

328

274

294

657

910

390

411

267

404

185

48.3

46.4

57.6

40.3

45.8

57.6

60.2

31.8

39.5

35.3

48.7

39.9

228

150

125

116

111

273

376

178

276

295

331

294

305

229

259

269

295

317

299

367

6.6

7.2

8.8

7.9

7.8

3.1

6.5

2.9

1.5

6.4

6.6

8.9

16.7

17.5

19.8

19.7

9.8

8.3

5.3

19.1

25.8

2.74 2.85 3.48 3.04 3.04 1.88 3.02 1.48 1.16 3.14 3.23 4.23

14.2

14.9

17.8

15.7

14.6

10.9

16.2

8.3

7.4

17.5

16.6

20.8

4.12 4.25 5.25 4.5

4.62 3.39 4.51 2.66 2.97 4.95 4.99 5.82

1.3

1.53 1.6

1.51 1.47 1.2

1.81 0.92 1.15 1.63 2.03 2.02

4.81 5.09 6.02 5.1

5.36 4.18 5.2

3.34 4.23 6.04 5.91 6.9

0.88 0.92 1.1

0.92 0.97 0.74 0.92 0.64 0.83 1.1

1.07 1.2

5.14 5.45 6.1

5.52 5.81 4.34 5.39 3.92 5.13 6.38 6.38 7.04

1.04 1.15 1.31 1.17 1.17 0.92 1.09 0.81 1.13 1.31 1.32 1.46

2.88 3.07 3.55 3.05 3.17 2.51 3.12 2.27 3.09 3.74 3.63 4.23

0.45 0.47 0.55 0.46 0.48 0.37 0.48 0.35 0.49 0.6

0.58 0.61

2.75 2.83 3.22 2.89 2.98 2.41 2.75 2.2

2.91 3.5

3.4

3.78

0.4

0.43 0.47 0.44 0.43 0.34 0.4

0.31 0.44 0.52 0.5

0.57

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Magnesium number varies in the narrow interval 45—53 for
the metamorphosed basalts, elevated values, up to 65, are typi-
cal for metagabbros/metagabbrodolerites. Titanium concen-
trations as a whole are low, not exceeding 2 wt. % TiO

in the

majority of samples do (max. 2.55 %). Furthermore, they de-
crease with an increasing magnesium number, where chromium
contents increase. In the case of nickel, however, the positive
correlation with magnesium number is weak. Potassium con-
tents are low ( < 0.2 wt. % K

O), slightly elevated concen-

trations  (max. 0.88 wt. %)  are  related  to  the  weak  secondary
biotitization.  We  used  trace  elements  generally  accepted  as
immobile  during  the  metamorphic  alteration,  namely  REE,
HFSE, Cr, V or Sc for reconstruction of the geochemical sig-
nature  of  the  metabasalts  and  geodynamic  setting  of  their
generation.  Chondrite  normalized  REE  patterns  for  meta-
basalts  from  the  Malá  Magura  Mts  (Fig. 6)  are  uniformly
mildly sloped (La

/Yb

= 1.63—1.86) and enriched in LREE in

comparison to mean oceanic N-MORB (La

= 27.85—37.13;

/Sm

= 1.00—1.10) resembling E-MORB types. The majority

of them also display a small Eu-anomaly (Eu/Eu*= 0.84—0.98).
The  REE  patterns  for  metabasalts  from  the  Suchý  Mts  are
more variable (Fig. 7). Types similar to N-MORB with low
total  REE  contents,  depletion  in  LREE  and  flat  form  of
HREE  patterns  (La

= 6.33—37.55; La

/Sm

= 0.32—0.96;

/Yb

= 0.87—1.61) can also be found there besides the

types identical to those from the Malá Magura Mts. However,
all these rocks with such different REE patterns belong petro-
graphically to metagabbros or metadolerites. Eu-anomalies
are absent or small (0.89—1.12). Geochemical signature close
to MORB for the metabasic rocks from the Suchý and Malá
Magura Mts can be deduced from the several traditionally used
discrimination diagrams such as Zr vs. TiO

(Pearce 1982),

Ti vs. V (Shervais 1982) or Y vs. Cr (Pearce 1982). The more
detailed specification of the geochemical type of these rocks

Fig. 4. Nb/Y vs. Zr/Ti diagram (Pearce 1996) for metabasic rocks from
the Suchý and Malá Magura Mts. Fields for their analogues from the
Pernek Group (Malé Karpaty Mts) were added for comparison. Data
for fields: Ivan et al. (2001), Ivan (2009) and unpublished data.

Fig. 5. TiO

vs. Al

diagram (Pearce 1983) for metabasic rocks

from the Suchý and Malá Magura Mts indicating similarity of their
composition to the mantle basaltic liquids or fractionated basalts.
Symbols and field – see Fig. 4.

Fig. 6. Chondrite normalized REE patterns for metabasic rocks
from the Malá Magura Mts. Normalization by McDonough & Sun
(1995), average N-MORB by Niu et al. (2002).

Fig. 7. Chondrite normalized REE patterns for metabasic rocks
from the Suchý Mts. Normalization by McDonough & Sun (1995),
average N-MORB by Niu et al. (2002).

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petrographic analogues from the Pernek Group (Malé
Karpaty Mts) displays identity or close similarity in all tes-
ted diagrams.

Major and trace element distributions in selected samples of

the metamorphosed carbonaceous sedimentary rocks from the
Suchý and Malá Magura Mts are presented in Table 2. High
contents of SiO

(75—88 wt. %) and C

tot

(3.5—11 wt. %, in-

cluding C

org

0.9—2.7 wt. %) as well as low contents of Al

( < 7 wt. %), Fe

tot

( < 1.8 wt. %), MgO ( < 0.7 wt. %), CaO

( < 0.1 wt. %), Na

O ( < 1 wt. %) and K

O (1.8 wt. %) are typi-

cal for graphitic gneisses and metacherts. Their position in the

Fig. 11. V-Cr-Zr diagram (Méres 2007) illustrating relatively high
content of V in the studied rocks similar to its analogues in the
Pernek Group and different composition of metamorphosed sedi-
mentary rocks in the Pezinok Group (both groups – the Malé Kar-
paty Mts). Symbols and fields – see Fig. 10.

Fig. 8. Zr vs. Y diagram (Le Roex et al. 1983) for metabasic rocks
from the Suchý and Malá Magura Mts. Field for their analogues
from the Pernek Group (Malé Karpaty Mts) was added for compari-
son. Symbols and data for field – see Fig. 4.

Fig. 9. Nb/Yb vs. Th/Yb diagram (Pearce & Peate 1995) for me-
tabasic rocks from the Suchý and Malá Magura Mts. Symbols and
fields – see Fig. 4.

Fig. 10. The Al

vs. SiO

plot (Méres 2007) indicating an ab-

sence of the chemical weathering and high contents of the SiO

the protolith of the graphitic gneisses and metacherts from the
Suchý and Malá Magura Mts. Fields for metamorphosed sedimentary
rocks of the Pernek and Pezinok Groups from the Malé Karpaty Mts
were added for comparison (see discussion for more details). Data
for graphitic gneisses and metacherts are taken from Table 2, fields
are based on data from Méres (2005, 2007).

in the Zr vs. Y diagram (Le Roex et al. 1983; Fig. 8) indicates
that  they  are  more  similar  to  E-MORB  than  to  N-MORB.
This fact is fully supported by the Nb/Yb vs. Th/Yb diagram
(Pearce  &  Peate  1995;  Fig. 9)  which  also  clearly  displays
some geochemical differences between metabasic rocks from
both crystalline cores – samples from the Malá Magura Mts
are  more  similar  to  typical  E-MORB  than  those  from  the
Suchý Mts. The same results can be obtained using Hf/3-Th-Ta
(Wood  1980),  Th-3Tb-2Ta  (Cabanis  &  Thiéblemont  1988)
or  La/10-Y/15-Nb/8  (Cabanis  &  Lecolle  1989)  discrimina-
tion  diagrams.  Comparison  of  the  studied  rocks  with  their

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Table 2: Major and trace element analyses of the metacherts and graphitic gneisses from
the Suchý and Malá Magura Mts. Note: Samples labelled MM – Malá Magura Mts, body
near the Chvojnica village; S – Suchý Mts, body in the Železná dolina valley.

Sample MM-05-1 MM-05-2 MM-05-3 MM-05-4

S-03-9 S-05-1 S-05-2

SiO

83.58 83.95 85.32 75.53 80.27 87.55 83.46

TiO

0.18 0.29 0.25 0.18 0.4

0.29 0.33

2.83 4.41 3.67 2.3

6.28 4.51 6.13

3tot

0.26 0.25 0.04 0.13 1.78 0.25 0.18

MnO

0.01 0.01 0.01 0.01 0.02 0.01 0.01

MgO

0.17 0.25 0.18 0.27 0.68 0.26 0.28

CaO

0.01 0.01 0.01 0.01 0.07 0.02 0.07

0.26 0.07 0.1

0.21 0.85 0.27 1.4

0.83 1.49 1.36 0.61 1.71 1.43 1.48

0.04 0.01 0.02 0.02 0.17 0.01 0.03

LOI

11.8

9.2

8.9

9.3

7.5

5.3

6.5

Total

99.97 99.94 99.86 88.57 99.73 99.9

99.87

tot

10.9

9.13 8.92 8.93 6.13 3.57 5.99

org

1.21 1.43 1.2

1.23 2.66 1.1

2.18

TOT/S

0.03 0.01 0.02 0.05 0.08 0.04 0.02

150

140

190

110

120

4.5

2.0

1.9

2.3

21.2

2.6

1.4

<0.5

1.4

0.6

0.5

1051

950

1279

756

498

522

733

36.2

35.1

36.2

23.6

36.2

38.9

37.9

387

752

464

274

830

1041

1246

9.3

3.5

5.4

7.7

24.1

10.7

33.5

0.2

0.4

0.2

0.3

0.2

0.3

3.1

3.5

2.8

2.6

3.1

2.4

3.4

1.5

2.1

1.5

1.3

2.5

2.4

3.1

85.3

121

97.4

83.2

99.6

96.6

128

64.8

82.1

68.7

61.1

38.6

39.2

10.7

2.2

2.6

2.8

1.4

3.3

1.6

10.5

9.4

9.8

8.6

4.3

4.1

Th/U

0.21 0.28 0.30 0.14 0.38 0.37 0.39

Th/Sc

0.22 0.22 0.23 0.16 0.33 0.12 0.11

12.5

16.5

13.7

7.6

11.8

2.8

1.5

18.1

24.5

20.4

10.5

20.2

4.6

2.5

3.14 4.57 3.71 2.18 3.29 0.81 0.42

14.0

19.7

16.3

9.0

14.0

3.8

2.0

3.1

4.6

3.7

2.1

3.0

1.3

0.5

0.54 0.67 0.61 0.34 0.65 0.22 0.05

4.64 6.54 5.3

4.23 3.72 2.46 0.93

0.88 1.26 1.03 0.92 0.74 0.56 0.19

6.01 8.39 6.81 6.33 4.44 4.34 1.2

1.52 2.1

1.69 1.54 1.05 1.11 0.28

5.1

6.53 5.32 4.81 3.39 3.37 1.00

0.76 0.96 0.84 0.73 0.5

0.58 0.19

5.54 7.21 5.75 5.39 3.21 3.6

1.26

0.86 1.08 0.95 0.82 0.56 0.58 0.26

/Yb

1.52 1.54 1.61 0.95 2.48 0.52 0.80

Eu/Eu*

0.44 0.37 0.42 0.35 0.57 0.37 0.23

et al. 2000; Dypvik & Harris 2001) are generally interpreted
as evidence for deposition in an extremely anoxic sedimen-
tary environment (Figs. 12 to 14). Taking into account addi-
tional geochemical ratios (Th/U, La/Sc, La/Y, La/Ce, Th/Sc)
and position in Th/Yb vs. Ta/Yb diagram (Fig. 15) lends fur-
ther support to a deep oceanic provenance of the sedimentary
protolith of the studied graphitic gneisses and metacherts. As
follows from the presented diagrams, all geochemical fea-
tures of the studied rocks are fully comparable with their pet-
rographic analogues from the Pernek Group but they are
distinctly different from the paragneisses and phyllites form-

ing the Pezinok Group – an adjoining
lithostratigraphic unit found in the Early
Paleozoic of the Malé Karpaty Mts.

Discussion

The crystalline complexes of the Suchý

and  Malá  Magura  Mts  together  with  the
crystalline  complexes  of  the  two  other
core mountains – the Malé Karpaty Mts
and Považský Inovec Mts, all located on
the  NW  margin  of  the  Tatric  megaunit,
differ from the rest of the Tatric megaunit
in some aspects of their geological struc-
ture and evolution. Presence of relatively
lower-grade  metamorphic  rocks,  clearly
intrusive relations of granitoids with sur-
rounding  rocks  or  a  common  occurrence
of  metamorphosed  basic  igneous  rocks
and  sedimentary  rocks  rich  in  organic
matter are among the most distinctive fea-
tures  of  the  mentioned  area,  sometimes
designated  as  the  Infratatric  unit  (e.g.
Plašienka  et  al.  1997).  The  most  pro-
nounced manifestations of all these pecu-
liarities are concentrated in the crystalline
core  of  the  Malé  Karpaty  Mts.  Two  dif-
ferent  lithostratigraphic  units  have  been
discerned  –  (1)  the  ophiolitic  Pernek
Group  and  (2)  the  volcano-sedimentary,
riftogeneous  Pezinok  Group.  They  form
an  integral  part  of  the  Variscan  and  Al-
pine  nappe  structures  (Ivan  et  al.  2001;
Ivan & Méres 2006).

Tectonically restricted bodies of the

metabasic rocks associated with the car-
bonaceous  metamorphosed  sedimentary
rocks  at  the  studied  localities  in  the
Suchý  and  Malá  Magura  Mts  represent
small  relics  of  specific  lithologies  pre-
served  in  the  complex  mosaic  of  the
present structure of this area. Integrity of
these  domains  is  indicated  not  only  by
the local preservation of original stratifi-
cation  (Fig. 2)  but  also  by  the  confor-
mity  of  fundamental  rock  parameters.
Metabasic rocks can be petrographically

classified as actinolite schists or amphibolites reflecting dif-
ferences in their metamorphic grade. Preserved relic textures
indicate that the starting rocks were a variegated association
of  basic  igneous  rocks  from  effusive  basalts  through
subvolcanic dolerites to intrusive gabbros (Fig. 3). As could
be inferred from the presence of stockwork of the metamor-
phosed hydrothermal veins, an intensive hydrothermal alter-
ation  preceded  regional  metamorphism  of  all  these  rocks.
Some rocks, mostly gabbros, underwent strong deformation
at  that  time.  Major  element  distribution  in  the  metabasalts
and  their  deep-seated  equivalents  indicate  that  they  crystal-

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lized from mostly less fractionated subalkaline tholeiitic ba-
saltic magmas (Fig. 4). Evidence of limited fractionation of
only  olivine  and  plagioclase  were  detected,  while  all  the
identified  metagabbros  belonged  to  the  isotropic  type
(Fig. 5).  The  distribution  of  trace  elements  generally  ac-
cepted as immobile in metamorphic processes (HFSE, REE)
indicates  that  original  basaltic  magmas  had  a  geochemical
signature close to the MORB-type. Metamorphosed basaltic
rocks from the Malá Magura Mts appear more uniform and
close  to  the  E-MORB  type  (Figs. 6  and  9),  whereas  those
from  the  Suchý  Mts  with  variable  trace  element  distribution
are much more similar to the typical N-MORB (Figs. 7 and 9).
The MORB-type geochemical signature of all these metabasic
rocks indicates an oceanic floor geotectonic setting.

Graphitic gneisses and metacherts are closely spatially re-

lated to metabasic bodies and do not occur isolated outside of
these  bodies.  As  follows  from  a  preserved  lithological  se-
quence in the metabasic body near Chvojnica village (Fig. 2),
the metamorphosed sedimentary rocks form the belt with the
stratiform  sulphide  mineralization  a  couple  of  dozens  of
meters in thickness. This belt is embedded in metabasic rocks
originally  represented  by  the  strongly  hydrothermally  altered
basalts. The geological situation is very similar to that in the
Pernek  Group,  where  several  analogous  belts  with  Cyprus-
type  sulphide  mineralization  are  present  (Cambel  1962;
Chovan  et  al.  1992;  Ivan  et  al.  2001).  Although  graphitic
gneisses rich in carbonaceous matter and quartz are the most
widespread  petrographic  type  of  metamorphosed  sediments
(Fig. 3E  and  F),  related  types  such  as  metacherts  or  quartz-
sericite  rocks  with  variable  content  of  carbonaceous  matter
and/or  tremolite/actinolite  are  also  present.  Impregnation  by
sulphide minerals (pyrite, rarely sphalerite) is ubiquitous in all
these  rock  types.  The  chemical  composition  of  graphitic
gneisses  and  metacherts  points  to  a  non-carbonate,  mostly
silica  dominated  sedimentation  in  strongly  anoxic  conditions
with variable supply of organic matter and clastic material of
the pelitic fraction. Such sedimentation is typical for a deep-
sea environment below CCD and the close spatial relations to
metabasalts of MORB signature localize it on the ocean floor
close to an active oceanic volcanic spreading center. The con-
tributions  of  several  sources  of  sedimentary  material  can  be
inferred  on  the  basis  of  trace  element  distribution.  Negative
Ce-anomaly  and  relative  enrichment  in  HREE  (Fig. 14)  re-
flect participation of an ancient seawater source (cf. Kato et
al.  2002),  whereas  values  of  other  geochemical  parameters
(Th/U<1, Th/Sc<0.25, La

/Yb

<6) and Ta/Yb vs. Th/Yb dia-

gram (Fig. 15) indicate a supply from the terrigenous source
resembling YUA (Young Undifferentiated Arc; McLennan et
al. 1993; Girty et al. 1996). The graphitic substance (with
partly preserved organic compounds) is a product of transfor-
mation of the organic matter accumulated in sediments due to
anoxic conditions which is also responsible for enrichment in
V, Cr and U (Figs. 11 to 13).

As mentioned above, the petrographic and geochemical

features of metabasic rocks as well as graphitic gneisses and
metacherts  from  the  Suchý  and  Malá  Magura  Mts  are  fully
comparable  with  those  from  the  Pernek  Group  in  the  Malé
Karpaty Mts. The Pernek Group has recently been identified
as  a  tectonically  reduced  Variscan  ophiolite  nappe  incorpo-

rated in the modern Alpine nappe structure, representing dis-
membered remnants of the uppermost part of the oceanic crust
profile  (Ivan  et  al.  2001;  Ivan  &  Méres  2003,  2006).  The
Pernek  Group  was  preliminarily  dated  as  ca.  370 Ma  old
(Putiš  et  al.  2009)  and  together  with  neighbouring  Pezinok
Group (Devonian) they were intruded and metamorphosed by
the ca. 350 Ma old granitoid plutons (Kohút et al. 2009). The
bodies  of  metabasic  rocks  associated  with  graphitic  gneisses
and metacherts in the Suchý and Malá Magura Mts probably
represent fault blocks of a Variscan ophiolite nappe identical
to  that  in  the  Malé  Karpaty  Mts.  Such  interpretation  is  also
supported by the existence of a similar fault block in the Malé
Karpaty  Mts,  located  in  the  granitoid  rocks  on  the  northern-
most  margin  of  the  crystalline  complex  (geological  map
1 : 50,000;  Maheq  et  al.  1970).  A  further  additional  support
also follows from the similarity of other lithologies adjacent
to  the  ophiolite  nappe  in  both  areas  –  granitoids  or
paragneisses. The geochemistry and intrusive age of the gra-
nitic rocks from the Suchý and Malá Magura Mts are close to
the  Bratislava  granitoid  massif  in  the  Malé  Karpaty  Mts
(Vilinovičová 1990; Kráq et al. 1997; Kohút et al. 2009) and
paragneisses  of  the  studied  area  strongly  resemble  those
from the Pezinok Group in the Malé Karpaty Mts in all sig-
nificant parameters (Méres 2007). Any amphibolitic rocks as
banded  amphibolites  or  retrogressed  eclogites  typical  for
complexes of the lower crustal origin (leptynite-amphibolite
complexes – LACs; e.g. Hovorka et al. 1997) have not been
found  there.  The  presence  of  ophiolitic  rocks  of  the  Pernek
Group  in  the  Suchý  and  Malá  Magura  Mts  is  an  important
additional  argument  for  the  specific  geological  structure  of
the “Infratatric unit”.

Domination of a geochemical signature close to E-MORB-

type  among  metabasalts  of  the  Pernek  Group  as  well  as  its
occurrence in the Suchý and Malá Magura Mts enables clas-
sification  of  this  ophiolite  nappe  as  a  relic  of  the  P-type
(Pearce 2008) or CM-type (CM – continental margin; Dilek
& Furnes 2011) of ophiolites. Such ophiolite type indicates as
a rule opening of the oceanic basin along the rifted continental
margins.  This  mechanism  probably  acted  in  the  case  of  the
studied rocks because of the spatial and time relations existing
between  the  Pernek  Group  and  the  Pezinok  Group  including
the typical rift-related volcanic rocks (Ivan et al. 2001).

Ophiolites of the same geochemical type, similar in age

and  lithology  to  the  Pernek  Group  have  also  been  found  in
the  Zlatník  and  Ochtiná  Groups  on  the  northern  margin  of
the  Gemeric  Superunit  in  the  inner  Western  Carpathians
(Fig. 1).  They  probably  represent,  together  with  the  Pernek
Group,  relics  of  a  single  Variscan  ophiolite  suture  tectoni-
cally dismembered in the Alpine era. This suture was created
as the last evolutionary stage of an oceanic basin termed as
the  Pernek  Ocean,  which  was  opened  as  a  result  of  rifting
probably in the Early Devonian and closed in the Late Devo-
nian/EarlyCarboniferous  time  (Ivan  &  Méres  2012,  2014).
The suture can be interpreted as a fossil boundary separating
two lithospheric paleoplates with different Variscan tectono-
thermal  evolution  where  the  southern  plate  (in  present  day
coordinates)  was  spared  extensive  plutonic  activities  and
metamorphic  reworking.  On  the  other  hand,  the  northern
plate displays a different history – the magmatic activity re-

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lated to the subduction of the Pernek Ocean and formation of
a  magmatic  arc  also  led  to  an  intensive  metamorphic  alter-
ation in the upper crust mainly due to increased thermal flow
and  related  granitoid  plutonism.  Late  Devonian/Early  Car-
boniferous (365—350 Ma) I- and S-type granitoids in the Vep-
oricum  and  Tatricum  Superunits  of  the  Western  Carpathians
could  be  the  products  of  this  plutonism  (cf.  Kohút  et  al.
2009; Broska et al. 2013).

The Variscan ophiolites identified in the Suchý and Malá

Magura  Mts  and  in  other  areas  of  the  Western  Carpathians
were formed during the oceanic basin opening and spreading
immediately before the main phase of the Variscan orogeny
in the Mississippian. Their analogues are known from several
localities  in  the  European  Variscides.  Variscan  ophiolites
Devonian in age have been described from NW Spain (Arenas
et al. 2007; Sánchez Martínez et al. 2007), Cornwall (Great
Britain  –  Clark  et  al.  1998),  Giessen  (Germany  –  Pin
1990), Vosges (France – Skrzypek et al. 2012) or from the
French Massif Central (Berger et al. 2006).

The paleogeographic position of the Pernek oceanic basin

still remains obscure and it could be solved in future by com-
parative studies of adjoining terrains concerning the place of
Pre-Miocene  docking  of  the  ALCAPA  block  (Eastern
Alps + Western Carpathians) somewhere in the vicinity of the
French  Massive  Central  (e.g.  Michalík  1994;  Stampfli  &
Hochard  2009).  The  Pernek  Ocean,  in  conformity  with  the
existing  global  tectonic  schemes,  can  be  interpreted  as  a
small oceanic basin formed by the active volcanic rifting in
the  leading  edge  of  the  Galatian  superterrane  as  a  result  of
roll-back  of  the  retreating  Rheic  Ocean  (Stampfli  et  al.
2013). Another possibility, based on a new interpretation of
the Variscan orogeny in the Eastern Alps, is its creation as an
embayment  of  the  Paleotethys  Ocean  progressively  scissor-
like  widening  to  the  east  in  the  present-day  coordinates
(Frisch et al. 2011).

Conclusions

The metamorphic rocks from the Suchý and Malá Magura

Mts previously known as amphibolites and graphitic gneisses
have been studied by field, petrographic and geochemical
methods. Interpretation of the results led us to the following
conclusions:

•

Small bodies composed of both mentioned rocks repre-

sent a specific lithology genetically different from the sur-
rounding crystalline rock complex;

•

Amphibolites, locally also actinolite schists, were formed

from effusive basalts, dolerites and isotropic gabbros by hy-
drothermal and following metamorphic alteration;

•

Metamorphosed basic igneous rocks display N- to

E-MORB geochemical signature typical for the oceanic floor
igneous rocks;

•

Graphitic gneisses to metacherts represent metamor-

phosed equivalents of non-carbonate siliceous sediments
with variable amount of organic matter;

•

Geochemical characteristics of metamorphosed sedi-

ments indicate a deep-sea sedimentary environment and a
combined oceanic water/terrigenous source of the sedimen-

tary material with the specific organic matter contribution
(enrichment in V, Cr, U) as a result of anoxic conditions;

•

The oceanic provenance of the studied rocks is a proof of

their ophiolitic character and oceanic crust affinity;

•

All relevant parameters correlate the studied rocks with

the ophiolitic Pernek Group, Devonian in age, widespread in
the Malé Karpaty Mts;

•

The small ophiolite bodies in the Suchý and Malá

Magura Mts could be interpreted as fault blocks created by
tectonic disintegration of the same Variscan ophiolite nappe
as that preserved in the Malé Karpaty Mts;

•

All the preserved Variscan ophiolites in the Western

Carpathians including those from the Suchý and Malá Magura
Mts belong to the continental margin type usually generated
by spreading in the rifted continental margin environment;

•

All the Variscan ophiolites in the Western Carpathians

originally  formed  an  integrated  suture  as  a  vestige  of  the
Pernek  Ocean  subducted  in  the  Lower  Carboniferous  and  a
fossil  boundary  between  two  lithospheric  paleoplates  with
different geological evolution in Variscan times.

Acknowledgments:  This  research  was  supported  by  VEGA
Grant  1/0555/13.  The  authors  are  indebted  to  Milan  Kohút
(D. Štúr State Geological Institute), Igor Petrík (Earth Science
Institute  of  the  Slovak  Academy  of  Sciences)  and  an  anony-
mous  reviewer  for  thorough  reviewing  this  manuscript,  their
suggestions and corrections are warmly acknowledged.

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