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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
04
—An
47
). 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
50
). 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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Fig. 3. Thin-section photomicrograph of metabasic rocks and graphite gneiss from the Suchý and Malá Magura Mts. A – Actinolite schist
containing actinolite (Act), albitic plagioclase (Pl), titanite/ilmenite (Ttn) and clinozoisite/epidote. Locality: Železná dolina Valley, Suchý
Mts, sample ASU-13; B – Phantom intersertal texture preserved in actinolite schist with pyrite (Py). Locality: Železná dolina Valley,
Suchý Mts, sample ASU-10; C – Relic ophitic texture in amphibolite composed mostly of brown magnesiohornblende (Mhb) and plagio-
clase (Pl). Locality: Chvojnica village, Malá Magura Mts, sample AMM-15; D – Relic granular texture in amphibolite with the brown
magnesiohornblende (Mhb). Locality: Chvojica village, Malá Magura Mts, sample AMM-19; E – Graphitic gneiss composed of musco-
vite (Ms), carbonaceous matter (c.m.) and quartz (Qz) with some plagioclase and pyrite. Locally also vanadian muscovite (roscoelite) is
present. Locality: Chvojnica village, Malá Magura Mts, sample MM-05-4; F – The same, crossed nicols.
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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
2
vs. SiO
2
(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
2
vs. Al
2
O
3
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
10
11
14
15
15A
1 5 6 7 8 12
13
SiO
2
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
2
1.72 1.84 2.12 1.84 1.89 1.53 1.87 1.18 1.35 2.26 2.23 2.55
Al
2
O
3
14.23 16.01 16.75 15.11 15.23 14.22 14.37 14.29 16.13 15.78 15.64 15.75
Fe
2
O
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
Na
2
O
2.75 3.30 3.28 2.97 2.99 2.42 1.70 2.85 3.09 3.71 4.07 2.98
K
2
O
0.55 0.29 0.18 0.44 0.31 0.18 0.55 0.44 0.87 0.15 0.12 0.28
P
2
O
5
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
C
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
S
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
Zr
108
112
140
115
127
99
136
73.8
65.5
155
154
186
Y
28.3
29.3
34
30.9
30.5
23.3
29
20.6
28.2
34.5
33.6
40.8
Hf
3
3.2
3.9
3.4
3.3
2.7
3.6
1.9
2
4.5
4
4.9
Th
0.7
0.8
0.7
0.6
0.7
<0.2
0.5
0.2
<0.2
0.3
0.3
0.3
U
0.3
0.3
2.3
0.2
0.2
0.1
0.7
0.1
0.9
0.1
0.2
0.8
Ta
0.5
0.5
0.6
0.6
0.5
0.2
0.4
0.1
<0.1
0.4
0.3
0.6
Nb
7.9
8.1
9.8
9
9.5
2.1
6.2
2.1
0.4
5
5
7.4
Cr
479
335
328
274
294
657
910
390
411
267
404
185
Co
48.3
46.4
57.6
40.3
45.8
57.6
60.2
31.8
39.5
35.3
48.7
39.9
Ni
228
150
125
116
111
273
376
52
59
87
178
63
Sc
34
36
40
36
36
35
33
42
51
40
41
40
V
276
295
331
294
305
229
259
269
295
317
299
367
La
6.6
7.2
8.8
7.9
7.8
3.1
6.5
2.9
1.5
6.4
6.6
8.9
Ce
16.7
17.5
22
19.8
19.7
9.8
18
8.3
5.3
18
19.1
25.8
Pr
2.74 2.85 3.48 3.04 3.04 1.88 3.02 1.48 1.16 3.14 3.23 4.23
Nd
14.2
14.9
17.8
15.7
14.6
10.9
16.2
8.3
7.4
17.5
16.6
20.8
Sm
4.12 4.25 5.25 4.5
4.62 3.39 4.51 2.66 2.97 4.95 4.99 5.82
Eu
1.3
1.53 1.6
1.51 1.47 1.2
1.81 0.92 1.15 1.63 2.03 2.02
Gd
4.81 5.09 6.02 5.1
5.36 4.18 5.2
3.34 4.23 6.04 5.91 6.9
Tb
0.88 0.92 1.1
0.92 0.97 0.74 0.92 0.64 0.83 1.1
1.07 1.2
Dy
5.14 5.45 6.1
5.52 5.81 4.34 5.39 3.92 5.13 6.38 6.38 7.04
Ho
1.04 1.15 1.31 1.17 1.17 0.92 1.09 0.81 1.13 1.31 1.32 1.46
Er
2.88 3.07 3.55 3.05 3.17 2.51 3.12 2.27 3.09 3.74 3.63 4.23
Tm
0.45 0.47 0.55 0.46 0.48 0.37 0.48 0.35 0.49 0.6
0.58 0.61
Yb
2.75 2.83 3.22 2.89 2.98 2.41 2.75 2.2
2.91 3.5
3.4
3.78
Lu
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
2
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
2
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
N
/Yb
N
= 1.63—1.86) and enriched in LREE in
comparison to mean oceanic N-MORB (La
N
= 27.85—37.13;
La
N
/Sm
N
= 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
N
= 6.33—37.55; La
N
/Sm
N
= 0.32—0.96;
La
N
/Yb
N
= 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
2
(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
2
vs. Al
2
O
3
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
2
(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
2
O
3
( < 7 wt. %), Fe
2
O
3
tot
( < 1.8 wt. %), MgO ( < 0.7 wt. %), CaO
( < 0.1 wt. %), Na
2
O ( < 1 wt. %) and K
2
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
2
O
3
vs. SiO
2
plot (Méres 2007) indicating an ab-
sence of the chemical weathering and high contents of the SiO
2
in
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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Al
2
O
3
vs. SiO
2
diagram (Fig. 10) indicates an absence of the
chemical weathering of the protolith. The high vanadium
content (Fig. 11) provides important clues for evaluation of
the original petrography and sedimentary environment of
these rocks. The enrichment in U (Fig. 12) and depletion in
Th, Sr, Ti and LREE as well are characteristic features of the
studied graphitic gneisses and metacherts in comparison
with other types of gneisses in the Suchý and Malá Magura
Mts (Table 2, Fig. 13) thought to be an equivalent of the
Pezinok Group from the Malé Karpaty Mts (Méres & Ivan
2008). Vanadium and uranium contents positively correlate
with C
tot
content. Low CaO and Sr contents suggest an ab-
sence of carbonates in the protolith and provide evidence of
non-carbonate sedimentary environments. Moreover, the
low Sr content together with low Ti content in metacherts is
an indication of the chemical/biochemical origin of their
protolith. PAAS normalized REE patterns display negative
Ce-anomaly, negative Eu-anomaly, low LREE/HREE ratio
and high HREE content (Fig. 14).
The occurrence of V-bearing minerals and U, Th, Cr and V
enrichment in metacherts together with the specific REE dis-
tribution (including negative Ce anomaly, McLennan 1989;
Sholkovitz & Schneider 1991; Holser 1997; Cullers 2002;
Kato et al. 2002), Th/U ratio (McLennan et al. 1993; Asiedu
Fig. 15. Th/Yb vs. Ta/Yb diagram for the graphitic gneisses and
metacherts from the Suchý and Malá Magura Mts. Fields for the
metamorphosed sedimentary rocks from the Pernek and Pezinok
Groups (both Malé Karpaty Mts) were added for comparison. Sym-
bols and fields for Pezinok and Pernek Groups – see Fig. 10. Others
fields after Cluzel et al. (2001).
Fig. 13. U-Th-Hf diagram (Méres 2007) indicated relatively high ura-
nium content in the graphitic gneisses and metacherts from the Suchý
and Malá Magura Mts. Similarity of these rocks to their analogues in
the Pernek Group and difference to metamorphosed sediments of the
Pezinok Group is obvious. Symbols and fields – see Fig. 10.
Fig. 12. Plot Th/U vs. Th (Méres 2007) indicates strong anoxic sed-
imentary environment of the graphitic gneisses and metacherts from
the Suchý and Malá Magura Mts. Symbols and fields – see Fig. 10.
Fig. 14. PAAS-normalized REE patterns of the graphitic gneisses
and metacherts from the Suchý and Malá Magura Mts. Fields for
the metamorphosed sedimentary rocks from the Pernek and Pezinok
Groups (both Malé Karpaty Mts) were added for comparison. Sym-
bols and fields – see Fig. 10. PAAS – Post-Archean average Aus-
tralian Shale (Taylor & McLennan 1985).
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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
2
83.58 83.95 85.32 75.53 80.27 87.55 83.46
TiO
2
0.18 0.29 0.25 0.18 0.4
0.29 0.33
Al
2
O
3
2.83 4.41 3.67 2.3
6.28 4.51 6.13
Fe
2
O
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
Na
2
O
0.26 0.07 0.1
0.21 0.85 0.27 1.4
K
2
O
0.83 1.49 1.36 0.61 1.71 1.43 1.48
P
2
O
5
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
C
tot
10.9
9.13 8.92 8.93 6.13 3.57 5.99
C
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
Cr
150
140
190
110
110
120
90
Ni
4.5
2.0
1.9
2.3
21.2
2.6
1.4
Co
<0.5
<0.5
<0.5
<0.5
1.4
0.6
0.5
Sc
10
12
12
9
10
13
14
V
1051
950
1279
756
498
522
733
Rb
36.2
35.1
36.2
23.6
36.2
38.9
37.9
Ba
387
752
464
274
830
1041
1246
Sr
9.3
3.5
5.4
7.7
24.1
10.7
33.5
Ta
0.2
0.4
0.2
0.2
0.3
0.2
0.3
Nb
3.1
3.5
2.8
2.6
3.1
2.4
3.4
Hf
1.5
2.1
1.5
1.3
2.5
2.4
3.1
Zr
85.3
121
97.4
83.2
99.6
96.6
128
Y
64.8
82.1
68.7
61.1
38.6
39.2
10.7
Th
2.2
2.6
2.8
1.4
3.3
1.6
1.6
U
10.5
9.4
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
La
12.5
16.5
13.7
7.6
11.8
2.8
1.5
Ce
18.1
24.5
20.4
10.5
20.2
4.6
2.5
Pr
3.14 4.57 3.71 2.18 3.29 0.81 0.42
Nd
14.0
19.7
16.3
9.0
14.0
3.8
2.0
Sm
3.1
4.6
3.7
2.1
3.0
1.3
0.5
Eu
0.54 0.67 0.61 0.34 0.65 0.22 0.05
Gd
4.64 6.54 5.3
4.23 3.72 2.46 0.93
Tb
0.88 1.26 1.03 0.92 0.74 0.56 0.19
Dy
6.01 8.39 6.81 6.33 4.44 4.34 1.2
Ho
1.52 2.1
1.69 1.54 1.05 1.11 0.28
Er
5.1
6.53 5.32 4.81 3.39 3.37 1.00
Tm
0.76 0.96 0.84 0.73 0.5
0.58 0.19
Yb
5.54 7.21 5.75 5.39 3.21 3.6
1.26
Lu
0.86 1.08 0.95 0.82 0.56 0.58 0.26
La
N
/Yb
N
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
N
/Yb
N
<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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Appendix
Location of samples presented in the paper:
AMM-10: amphibolite, Malá Magura Mts, Chvojnica village. GPS coordinates: N 48°53.598’, E 018°33.065’, 562 m a.s.l.
AMM-11: amphibolite, Malá Magura Mts, Chvojnica village. GPS coordinates: N 48°53.598’, E 018°33.074’, 562 m a.s.l.
AMM-14: amphibolite, Malá Magura Mts, Chvojnica village. GPS coordinates: N 48°53.389’, E 018°33.344’, 646 m a.s.l.
AMM-15: amphibolite, Malá Magura Mts, Chvojnica village. GPS coordinates: N 48°53.394’, E 018°33.328’, 644 m a.s.l.
AMM-15A: amphibolite, like AMM-15, 1 m to the N, GPS coordinates: N 48°53.394’, E 018°33.328’, 644 m a.s.l.
AMM-19: amphibolite, Malá Magura Mts, Chvojnica village. GPS coordinates: N 48°53.503’, E 018°33.209’
ASU-1: amphibolite, Suchý Mts, Nevidzany village, valley of the Krstenica brook.
GPS coordinates: N 48°53.503’, E 018°33.209’
ASU-5: amphibolite, like ASU-1 GPS coordinates: N 48°53.503’, E 018°33.209’
ASU-6: amphibolite, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley (valley of the Závada brook).
GPS coordinates: N 48°50.270’, E 018°21.906’
ASU-7: amphibolite, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley.
GPS coordinates: N 48°50.240’, E 018°21.844’
ASU-8: amphibolite, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley.
GPS coordinates: N 48°50.631’, E 018°22.339’
ASU-10: actinolite schist, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley.
GPS coordinates: N 48°50.587’, E 018°22.252’
ASU-12: actinolite schist, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley.
GPS coordinates: N 48°50.584’, E 018°22.586’, 437 m a.s.l.
ASU-13: actinolite schist, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley.
GPS coordinates: N 48°50.581’, E 018°22.308’, 489 m a.s.l.
MM-05-1: metachert, Malá Magura Mts, Chvojnica village. GPS coordinates: N 48°53.490’, E 018°33.209’
MM-05-2: metachert, like MM-05-1
MM-05-3: metachert, Malá Magura Mts, Chvojnica village. GPS coordinates: N 48°53.522’, E 018°33.280’
MM-05-4: metachert, like MM-05-3
S-03-9: graphitic gneiss, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley.
GPS coordinates: N 48°50.654’, E 018°22.210’
S-05-1: metachert, Suchý Mts, Závada pod Čiernym vrchom village, Železná dolina valley.
GPS coordinates: N 48°50.479’, E 018°22.375’
S-05-2: metachert, like S-05-1.