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, OCTOBER 2015, 66, 5, 375—391 doi: 10.1515/geoca-2015-0032
Introduction
The Northern Gemeric Unit (NGU) Permian volcanic-sedi-
mentary succession overlaps unconformably with eroded rel-
ics of the Carboniferous sedimentary sequences as well as
the two pre-Carboniferous crystalline basement complexes,
the Rakovec and Klátov Complexes. These Paleozoic com-
plexes, in the northern and north-eastern part of the Sloven-
ské Rudohorie Mts, are located in a very complicated Alpine
synclinorium structure, in which the system of folds, tec-
tonic slivers and fold faults is cut by younger transversal tec-
tonics (Bajaník et al. 1983, 1984; Biely et al. 1996a and
references therein). As the Permian sedimentation proceeded
from continental arid to semiarid climatic conditions, they
lack or are deprived of relevant faunal and floral age evi-
dence. In addition, the Alpine deformation and anchi- to
low-grade metamorphic recrystallization destroyed the ma-
jority of possibly pre-existing biostratigraphically relevant
fossil remains. Because a distinct part of the Permian se-
quence is formed by acidic to intermediate metavolcanic
rocks and their volcanoclastics, they could be used to prove
the age of these volcanic horizons, as well as for age estima-
tion of the adjoining sediments.
The first U-Pb dating from the U-bearing volcanogenic
horizon within the Novoveská Huta ore deposits gave the
First evidence for Permian-Triassic boundary volcanism in
the Northern Gemericum: geochemistry and U-Pb zircon
geochronology
ANNA VOZÁROVÁ
1
, SERGEY PRESNYAKOV
2
, KATARÍNA ŠARINOVÁ
1
and MILOŠ ŠMELKO
1
1
Comenius University in Bratislava, Faculty of Natural Sciences, Department of Mineralogy and Petrology, Ilkovičova 6, Pav. G, 842 15,
Bratislava, Slovak Republic; vozarova@fns.uniba.sk; sarinova@fns.uniba.sk; smelko@fns.uniba.sk
2
A.P. Karpinsky Russian Geological Institute (VSEGEI), Sredny prospect 74, 199 106 St.-Petersburg, Russia; Sergey_Presnyakov@vsegei.ru
(Manuscript received March 5, 2015; accepted in revised form August 10, 2015)
Abstract: Several magmatic events based on U-Pb zircon geochronology were recognized in the Permian sedimentary
succession of the Northern Gemeric Unit (NGU). The Kungurian magmatic event is dominant. The later magmatism stage
was documented at the Permian-Triassic boundary. The detrital zircon assemblages from surrounding sediments docu-
mented the Sakmarian magmatic age. The post-orogenic extensional/transtensional faulting controlled the magma ascent
and its emplacement. The magmatic products are represented by the calc-alkaline volcanic rocks, ranging from basaltic
metaandesite to metarhyolite, associated with subordinate metabasalt. The whole group of the studied NGU Permian
metavolcanics has values for the Nb/La ratio at (0.44—0.27) and for the Nb/U ratio at (9.55—4.18), which suggests that they
represent mainly crustal melts. Magma derivation from continental crust or underplated crust is also indicated by high
values of Y/Nb ratios, ranging from 1.63 to 4.01. The new
206
U—
238
Pb zircon ages (concordia age at 269 ± 7 Ma) confirm
the dominant Kungurian volcanic event in the NGU Permian sedimentary basin. Simultaneously, the Permian-Triassic
boundary volcanism at 251 ± 4 Ma has been found for the first time. The NGU Permian volcanic activity was related to a
polyphase extensional tectonic regime. Based on the new and previous U-Pb zircon ages, the bulk of the NGU Permian
magmatic activity occurred during the Sakmarian and Kungurian. It was linked to the post-orogenic transpression/transtension
tectonic movements that reflected the consolidation of the Variscan orogenic belt. The Permian-Triassic boundary magmatism
was accompanied by extension, connected with the beginning of the Alpine Wilson cycle.
Key words: zircon (SIMS) ages, acid to intermediate volcanites, North Gemeric Permian basin, Western Carpathians.
age of 240 ± 30 Ma, that was interpreted as the age of miner-
alization (Arapov et al. 1984). Monazite ages prove the Ci-
suralian age of 278 ± 10Ma in the metarhyolite tuff from the
same locality (Rojkovič & Konečný 2005). The newest U-Pb
(SHRIMP) magmatic zircon ages from the NGU Permian
volcanic suite (in the vicinity of Krompachy) yielded the
concordia age of 272 ± 7 Ma for basaltic metaandesite, and the
concordia age of 275 ± 4 Ma for metarhyodacite (Vozárová
et al. 2012). These results also correspond to the Cisuralian
Epoch, in the time span of the Kungurian Stage. Conse-
quently, the acquired
206
Pb/
238
U zircon age data document
nearly a contemporaneous manifestation of the acid and ba-
sic volcanic activity within the NGU Permian basin.
Therefore, our investigation focuses on the continuation of
magmatic zircon radiometric dating in order to confirm the
stratigraphic specification and position of the subdivided
lithostratigraphic units. The method of in situ U-Pb SHRIMP
zircon dating (performed at the A.P. Karpinsky Russian
Geological Institute (VSEGEI), Laboratory of Isotopic Re-
search, St.-Petersburg) has been applied, with the main tar-
get of determining the age of volcanism and specifying the
stratigraphic position of the adjoining sediments. In this
study, we follow the time-scale calibration of the Interna-
tional Stratigraphic Chart 2014 (International Commission
on Stratigraphy, drafted by Cohen et al. 2014) in order to
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compare geochronological data from the studied volcanics
with the fossil-bearing strata. The main goal of this study
was to bring new isotopic and geochemical data on the
sources of magma generation, in order to infer the relation-
ship with the geotectonic setting of the studied area.
Geological setting
The NGU belongs to the pre-Gosau northward stacking
crustal scale nappe system of the Western Carpathians (Biely
et al. 1996a and references therein). The NGU fits into the
innermost part of the internal zone of the Alpine Western
Carpathians, and as a whole it clearly overthrusts the Vepori-
cum Unit in its footwall, along the Alpine thrust nappe con-
tact recognized as the Lubeník-Margecany Line (Andrusov
1959). Similarly, further to the south, the tectonic contact of
the NGU with the neighbouring Southern Gemericum Unit is
represented by the Hrádok-Železník Line (defined by Abonyi
1971), which continues the system of thrust faults to the east
(Fig. 1). Extreme Early Cretaceous shortening due to nappe
stacking is characteristic for the innermost part of the West-
ern Carpathians. Due to this fact, the complexes preserved in
the NGU synclinorium (Mahet 1954; Mahet & Malkovský
1984) structure are generally specified by the strong tectonic
reduction and shortening.
The NGU zone encloses relics of the Variscan collision su-
ture, represented by the thrust wedges of the two pre-Car-
boniferous complexes (the higher-grade Klátov and low-grade
Rakovec Terranes; in the sense of Vozárová & Vozár 1996),
and fragments of Mississippian deep-water turbidite se-
quences (Fig. 1).
The NGU Mississippian turbidite wedges (the Ochtiná
Group divided into the Hrádok, Črmet and Lubeník Forma-
tions in the sense of Vozárová 1996), supposedly disposed
by the Variscan suture, represent the intra-suture remnant of
the ocean basin fill. The turbidite deposition (the Hrádok and
Črmet Formations) was followed by the deposition of
Visean/Serpukhovian shallow water clastics and carbonates
(the Lubeník Formation). The Tournaisian—Visean fore-deep
and remnant ocean basins have been correlated across the
whole Alpine-Carpathian realm (Nötsch-Veitsch-Northge-
meric Zone – Neubauer & Vozárová 1990; Veitsch/Nötsch-
Szabadbattyán-Ochtiná Zone – Ebner et al. 2008). They are
partly syn-orogenic, and partly also post-date the Late Devo-
nian—Mississippian climax of the Variscan orogeny.
Post-Variscan deposition includes Pennsylvanian (Bashki-
rian—Lower Moscovian) fan delta/shallow-marine to proximal
delta (Upper Moscovian—Kasimovian) and continental Per-
mian sequences (Rakusz 1932; Rozlozsnik 1935; Rozložník
1963; Bajaník et al. 1981, 1983; Vozárová & Vozár 1988;
Vozárová 1996 and references therein).
Fig. 1. Schematic geological map of the NGU showing the volcanic rock sampling localities (modified from the Geological map of Slovakia,
1 : 500,000, Biely et al. 1996b). The red line squared field designes the area of zircon collecting. For more details see Fig. 12.
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Shallow-water to paralic Upper Bashkirian-Moscovian for-
mations overstepped unconformably both, the NGU pre-Car-
boniferous crystalline complexes (Klátov and Rakovec T.) as
well as, the Mississippian syn-orogenic Črmet Formation in
the eastern part of the occurrences (a part of the Veitsch/
Nötsch-Szabadbattyán-Ochtiná Zone; Ebner et al. 2008). Im-
portant indications are two breaks of sedimentation. The first
was during the Early Pennsylvanian (Bashkirian) and the sec-
ond in the Late Pennsylvanian (Kasimovian—Ghzelian). Both
hiati were connected with gradual reconstruction of the NGU
sedimentary realm, at the first stage in a transpressional and
the second in a transtensional tectonic setting (Vozárová et al.
2009a). This assumption is documented by a different pre-
transgressive erosion step of individual pre-Pennsylvanian se-
quences and by their reworked detrital material. The marine
post-orogenic sequence (8—170 m thick) started with delta-
fan boulder to coarse-grained polymict conglomerates (the
Rudňany Formation), with rock fragments derived from all
the pre-Pennsylvanian complexes of the NGU zone. The
370—380 Ma
40
Ar/
39
Ar cooling age data from sandstone clas-
tic white mica and gneiss pebble metamorphic mica, as well as
the detrital zircon ages (Vozárová et al. 2005, 2013) indicate
perfectly the first step of the Variscan collisional suturing in
NGU realm. After initial rapid sedimentation, the littoral to
shallow-neritic limestones and fine-grained siliciclastic sedi-
ments were associated with basalts and their volcanoclastics.
This succession was formerly defined as the Zlatník Forma-
tion (ZF) by Bajaník et al. (1981). The lower part of the ZF is
well biostratigraphically fixed, based on brachiopods, bryozo-
ans, crinoids, gastropods, corals, ammonites and mainly trilo-
bites (Rakusz 1932; Bouček & Přibyl 1960), plant debris
(Němejc 1953) and conodonts (Kozur & Mock 1977).
Ivan & Méres (2012) separated the complex of basic
metavolcanites and metavolcanoclastics, associated with
small amounts of metapelites and fine-grained metapsammites
from the lower part of the ZF. The metabasalts of E-MORB,
N-MORB and BABB types in this complex and chemical dif-
ferences in these rocks were considered to be the basis for the
separation of these metabasalts from the lower part of the ZF.
The authors defined this new lithostratigraphic unit as the
Zlatník Group. However, this name expression was firstly
used for the biostratigraphically well assessed ZF (Bajaník et
al. 1981). This strongly contradicts the priority rule of the
stratigraphic code (see the International Guide to Stratigraphic
Classification; Hedberg 1976 and others; Slovak Stratigraphic
Guide, Michalík et al. 2007). According to the definition of
the new lithostratigraphic unit rule, as defined by Ivan &
Méres (2012), the detailed field distinction of the Zlatník
Group and, above all, its relationship to underlying and over-
lying rock complexes (tectonic or primary position etc.) are
missing. Though the schematic map was presented, it seems
that the authors included in the Zlatník Group even some parts
of the Rakovec Group and the Rudňany Formation rock
complexes. For the solving of this problem, further structural
and geological field studies are badly needed. In any case,
only the geochemical data cannot form the basis for such dis-
tinction. The submitted work is not going to form any argu-
ments for further solving of this problem, as the ZF succession
in the eastern part of the NGU is not present.
The termination of this Late Bashkirian—Moscovian pe-
ripheral basin is reflected by cyclical paralic sedimentation
(the Hámor Formation).
The continental Permian deposits (Krompachy Group;
Bajaník et al. 1981) overlap the slightly deformed Pennsyl-
vanian and Mississippian sedimentary rocks, as well as both
NGU pre-Carboniferous crystalline rock complexes. The
basal Knola Formation (KF) contains poorly sorted polymict
conglomerates of variable thickness (Fig. 2), with pebbles
derived from the directly underlying rock complexes. Acid
to intermediate/basic volcanism associated with the red-beds
of fluvial, fluvial-lacustrine and playa facies is characteristic
of the Petrova hora Formation (PHF) (Fig. 2). The existing
monazite and U-Pb SHRIMP zircon ages yield a Cisuralian
age (Artinskian—Kungurian) for both, the acidic and basic vol-
Fig. 2. Schematic lithostratigraphic column of the NGU Permian se-
quence (modified after Bajaník et al. 1981; Vozárová 1996 and this
study). The time-scale calibration follows the International Strati-
graphic Chart (International Commission on Stratigraphy, drafted by
Cohen et al. 2014).
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canic members (Rojkovič & Konečný 2005; Vozárová et al.
2012). The acidic volcanism produced the huge mass of pyro-
clastic rocks, mainly in the eastern part of the NGU. Two re-
gional pulses of volcanic activity correspond to the
large-scale sedimentary cycles triggered by the extensional
regime. Based on these two independent volcanogenic hori-
zons, some authors determined two separate lithostratigraphic
members within the PHF: i) the older Novoveská Huta vol-
canic complex, and ii) the younger Pátrov Grúň volcanic
complex (Novotný & Mihát 1987; Mihát 1990 in Rojkovič
& Mihát 1991). The PHF volcanism was usually dominated
by the metarhyolite-dacite volcanic rocks, associated with
metaandesite and basaltic metaandesite (Ivanov 1953, 1957;
Mahet 1954; Rojkovič & Vozár 1972; Václav & Vozárová
1978; Novotný & Mihát 1987; Rojkovič & Mihát 1991;
Vozárová et al. 2012).
The top of the Permian succession (Fig. 2) consists of the
Novoveská Huta Formation (NHF) red-beds that prograded
upwards and across to near-shore sabkha/lagoonal evaporite
facies.
Analytical methods
Zircons have been separated from rocks by standard grind-
ing, heavy liquid and magnetic separation procedures. The
internal zoning structures and shapes of the half-sectioned
zircon crystals mounted in epoxy resin puck with chips of
the TEMORA (Middledale Gabbroic Diorite, New South
Wales, Australia, Black et al. 2003) and 91500 (Geostandard
zircon, Wiedenbeck et al. 1995) reference zircons, were im-
aged by optic microscopy, BSE and CL, in order to guide an-
alytical spots positioning. In situ U-Pb analyses were
performed on a SHRIMP-II in the Centre of Isotopic Re-
search (CIR) at VSEGEI in St.-Petersburg, Russia.
Each analysis consisted of 5 scans through the 196—254
AMU (atomic mass range); primary beam diameter was
about 25 µm, with intensity of ca. 6 nA. The data have been
reduced in a manner similar to that described by Williams
(1998 and references therein), using the SQUID Excel Macro
of Ludwig (2000). The Pb-U ratios have been normalized
relative to a value of 0.0668 for the
206
Pb/
238
U ratio of the
TEMORA reference zircons, equivalent to an age of 416.75 Ma
(Black et al. 2003); common lead was corrected using mea-
sured
204
Pb/
206
Pb (Stacey & Kramers 1975). Age calcula-
tions and plotting were done with ISOPLOT/EX (Ludwig
1999). Uncertainties given for individual analyses (ratios
and ages) are at the one
σ level; however, the uncertainties in
calculated Concordia ages are reported at the two
σ levels.
The chemical composition of the rocks was analysed at the
ACME Analytical Laboratories (Vancouver, Canada). Major
elements were determined by inductively coupled plasma –
optical emission spectrometry (ICP-OES). Concentrations of
trace elements and rare earth elements (REE) were deter-
mined by ICP mass spectrometry (ICP-MS). The analytical
accuracy was controlled using geological standard materials
and is estimated to be within a 0.01% error (1
σ, relative) for
major elements, within a 0.1—0.5 ppm error range (1
σ, rela-
tive) for trace elements and 0.01—0.05 ppm for REEs. Fur-
ther details are accessible on the web page of the ACME Ana-
lytical Laboratories (http://acmelab.com/).
Sample characteristics
Petrography
The acidic members of the PHF volcanics represent a rela-
tively huge volcanic succession related to subaerial fissure
eruptions. Pyroclastic tuffs and ignimbrites are dominant with
subordinate lava flows. The huge aerial eruptions are also doc-
umented by mixing of large redeposited volcanoclastic detri-
tus with the surrounding non-volcanic sediments. The acidic
volcanics are characterized by the prevalence of vitric matrix
and less preserved phenocrysts of
β-quartz, K-feldspar and
Na-plagioclase. Relics of deeply altered biotite are scarce. A
relative strong Alpine reworking is manifested by distinct foli-
ation and preferred orientation of the newly-formed aggre-
gates of muscovite + albite + quartz ± chlorite.
The PHF intermediate to basic volcanic members are rep-
resented by metaandesites and basaltic metaandesites, less
metabasalts. They are fine-grained violet or dark-green rocks
with dominant glassy, microofitic or vitroporphyric texture.
Lathes of plagioclases are the dominant phenocrysts. Albi-
tized plagioclases with inclusions of chlorite/illite were also
observed. Magmatic mafic minerals are completely decom-
posed and replaced by Fe-Mg chlorite and Fe-Ti oxides.
Magnetite and ilmenite belong to the primary mafic minerals.
Ilmenite was partially decomposed to rutile and hematite.
The strong Alpine deformation and recrystallization are re-
flected in the fine-grained aggregates of chlorite + Fe-Ti
oxides + calcite + epidote ± albite, which crystallized along
the foliation planes. The acidic volcanics are dominant in the
northern and north-eastern part of the Slovenské Rudohorie
Mts and more basic volcanics in its eastern part, mainly at
the localities of Krompachy and Jahodná.
Three samples have been collected, GZ-32, GZ-33 and
GZ-34, for zircon dating, all from the vicinity of Jahodná,
northwest from Košice. Among them, only two samples (GZ-32
and GZ-33) were suitable for dating. The first, GZ-32 sample
(GPS: N 48°45’810”, E 21°09’000”; 607 m above sea level;
ca. 250 m east of the Kuríšková (622 m) elevation point)
represents the acid variety, corresponding to the fine-grained
metarhyodacite or metadacite pyroclastic rock, beige in co-
lour. No phenocryst relics are preserved and thus, due to the
very strong Alpine deformation and recrystallization, it is
difficult to distinguish if the original rock was primary apha-
nitic volcanic or felsic pyroclastic rock. A very strong folia-
tion is also reflected in the distinct preferred orientation of
the newly formed metamorphic minerals in the texture (mus-
covite + albite + quartz ± chlorite). Irregular dispersed Fe-Ti
oxide grains are preserved in the fabric.
The second sample, GZ-33 (GPS: N 48°45’411”,
E 21°09’746”; 551 m above sea level; ca. 350 m NW from
the Kamenný hrb (559 m) elevation point), corresponds to a
dacite/andesite composition. The studied volcanic rock is
dark, dark-violet in colour and with microporphyritic texture.
It is fine-grained, macroscopically with small whitish plagio-
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clase phenocrysts, which are deformed and cataclasitized
within the foliated matrix. An intersertal or fluidal texture,
dominated by lathes of plagioclase (albite), was partly identi-
fied in the basaltic andesite rocks (sample GZ-34). Spaces be-
tween plagioclase lathes are filled with fine-grained chlorite
and chlorite/muscovite masses after primary glassy material.
The plagioclase grains are strongly albitized. The metaandes-
ites and basaltic metaandesites are characterized by plentiful
grains of Fe-Ti oxides within the fine-grained matrix, and less
frequent phenocrysts of magnetite and ilmenite.
Geochemistry
The NGU Permian volcanic rocks include a wide range of
compositions, ranging from basaltic andesite, andesite to
dacite and rhyolite. Representative major- and trace-elements
including rare earth elements of whole-rock analyses are given
in Tables 1 and 2. The list of the analysed volcanic rocks and
sample localities is specified in Table 3. The NGU Permian
volcanic rocks vary from peraluminous to metaluminous in-
termediate to acid volcanic suite. The loss on ignition (LOI)
suggests the variable degrees of post-magmatic alteration
(3.9—2.6 wt. % of volatiles). The degree of secondary alkali
metasomatic alteration has been considered by reference to
the variation of total alkali content to potash/total alkali ratio
(Hughes 1973, 1982). Generally, the NGU metaandesites and
basaltic metaandesites, associated with a part of the metarhyo-
dacites (Group I.) belong to the unaltered or slightly Na-meta-
somatically altered volcanic rocks (Na
2
O + K
2
O ranging from
6.3 to 8.3; K
2
O/Na
2
O + K
2
O*100 ranging from 21 to 55).
A second part of the metarhyodacites (Group II.) is indicated
by their lower total alkali content (Na
2
O + K
2
O ranging from
Andesites Rhyolites-dacites
Fm
PH PH PH PH PH NV PH PH PH NV
Sample
14 sm
16 sm
20 sm
21 sm
41 sm
GZ-34
15 sm
17 sm
GZ-32 GZ-33
SiO
2
%
60.26
55.94
57.1
55.51
58.19
60.76
68.31
68.54
66.98
64.31
TiO
2
0.97
1.19
1.08
1.15
1.03
1.00
0.32
0.27
0.22
0.44
Al
2
O
3
16.45
16.07
15.85
15.82
18.02
16.66
15.99
16.17
15.26
15.82
Fe
2
O
3
7.66
9.02
8.96
9.47
8.25
6.20
4.18
4.59
4.38
6.53
MnO
0.11
0.09
0.11
0.11
0.04
0.04
0.03
0.12
0.04
0.02
MgO
1.97
1.85
1.99
2.01
3.45
3.75
0.86
0.35
3.27
2.26
CaO
1.79
3.58
3.48
4.19
0.62
0.58
0.21
0.33
0.22
0.31
Na
2
O
5.28
4.91
4.49
4.78
5.38
7.14
5.99
4.27
0.60
4.15
K
2
O
2.32
1.75
2.15
1.50
1.42
0.42
2.36
2.97
5.16
3.02
P
2
O
5
0.395 0.604 0.560 0.596 0.420 0.440 0.147 0.088 0.130 0.210
Cr
2
O
3
n.d.
n.d.
n.d.
n.d.
0.002
n.d.
n.d.
n.d.
n.d.
0.005
LOI
2.7
5.0
4.2
4.9
3.0
2.9
1.5
2.2
3.6
2.7
sum
99.89
100.03
99.99
100.02
99.81
99.86
99.87
99.88
99.85
99.8
Rb
ppm
91.3
59.8
67.5
50.3
51.3
16.7
81.8
105.5
146.6
106.9
Cs
5.0
2.1
2.7
1.5
2.8
0.9
4.2
3.4
8.5
4.5
Ba
453
209
283
153
113
69
320
283
158
147
Sc
13
15
15
16
15
13
9
9
7
12
Y
43.0
46.4
44.6
46.2
34.5
41.5
66.8
60.1
54.2
58.2
La
27.8
35.8
36.7
37.8
23.3
35.3
64.6
77.5
47.0
76.2
Ce
63.5
79.5
80.7
82.4
57.5
78.8
132.1
138.7
109.6
179.1
Pr
8.45
10.55
10.54
10.71
6.91
9.13
16.84
18.03
13.01
20.87
Nd
36.5
44.0
43.0
43.6
29.7
37.9
67.4
66.5
52.9
77.0
Sm
7.92
9.00
8.73
8.99
7.42
8.36
12.91
11.41
12.98
15.59
Eu
1.84
1.98
2.02
2.22
1.55
1.92
2.51
2.23
2.10
2.91
Gd
8.05
8.87
8.4
8.64
7.54
8.38
12.38
10.57
10.66
13.8
Tb
1.34
1.42
1.38
1.43
1.25
1.16
2.00
1.64
1.44
1.71
Dy
7.60
8.20
8.11
7.98
6.95
7.78
11.42
9.00
9.74
12.5
Ho
1.59
1.67
1.60
1.64
1.36
1.42
2.35
1.93
1.76
2.14
Er
4.39
4.64
4.47
4.60
3.72
4.24
6.82
5.64
5.39
6.27
Yb
4.11
4.45
4.34
4.36
3.50
3.91
6.78
5.27
5.10
5.84
Lu
0.64
0.70
0.66
0.67
0.50
0.61
1.10
0.86
0.75
0.96
Th
8.7
9.7
9.0
8.9
10.0
7.3
19.4
19.7
11.7
17.7
U
2.6
2.4
2.5
2.4
3.2
2.8
4.8
3.1
2.6
4.0
V
72
57
43
52
89
68
9
n.d.
n.d.
n.d.
Co
12.9
13.5
12.5
13.8
14.0
15.6
1.7
1.4
2.7
3.2
Ni
1.5
1.5
1.8
0.8
1.6
1.1
1.1
1.6
0.7
2.7
Zr
232
279
276.3
268.6
296
239.4
568.4
478.4
314.8
569.4
Nb
11.8
14.1
13.0
13.1
14.8
11.7
22.8
14.1
13.5
20.3
Hf
6.4
7.6
7.4
7.0
8.3
6.3
14.6
12.0
8.4
13.3
Ta
0.8
0.9
0.8
0.9
1.1
0.9
1.4
0.9
1.1
1.3
Ga
20.9
20.3
18.4
18.0
24.4
22.2
21.2
22.5
22.5
23.6
Pb
2.0
0.9
6.7
0.9
2.3
0.8
3.1
0.8
0.7
1.1
Eu/Eu*
0.702 0.675 0.719 0.767 0.699 0.631 0.605 0.618 0.544 0.604
Table 1: Chemical composition of the Group I volcanic rocks, basaltic andesite-rhyolite suite with Eu/Eu* > 0.5. Analysis 16 sm has been
selected from Vozárová et al. (2012). PH – Petrova hora Formation, NV – Novoveská Huta Formation.
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2.6 to 5.3) and high potash/alkali ratio (K
2
O/Na
2
O + K
2
O*100
ranging from 94 to 97) which is typical for K-metasomatism.
In order to minimize the effect of post-magmatic alteration,
interpretation is mainly based on the immobile elements.
The NGU metavolcanics are classified on the basis of incom-
patible elements Zr/Ti vs. Nb/Y (after Pearce 1996). They as-
semble a continuous volcanic suite from the metarhyolite
and metadacites to metaandesite and basaltic metaandesites and
plot in the subalkaline field (Nb/Y < 0.70; Fig. 3). The Mg-num-
bers of the NGU metaandesites and metarhyodacites have
Table 2: Chemical composition of the Group II volcanic rocks, rhyolite-dacite suite with Eu/Eu* > 0.5. Analyses 38 sm and 38 sm-b have
been chosen from Vozárová et al. (2012). PH – Petrova hora Formation.
Rhyolites-dacites
Fm
PH PH PH PH PH PH PH PH
Sample
19 sm
25 sm
33 sm
34 sm
36 sm
38 sm
38 sm-b
39 sm
SiO
2
%
74.93 80.69 71.62 72.11 79.55 82.50 80.95 71.54
TiO
2
0.17
0.44
0.30
0.05
0.06
0.12
0.12
0.12
Al
2
O
3
12.52 9.17 12.79 15.99 12.23 8.75 11.02 13.88
Fe
2
O
3
3.16 3.42 3.04 1.08 1.59 2.25 2.22 1.53
MnO
0.01 0.01 n.d n.d 0.04 n.d. 0.03 0.04
MgO
3.03 0.51 2.82 3.31 0.74 1.71 0.30 2.30
CaO
0.11 n.d. 0.04 0.02 n.d 0.04 0.07 1.43
Na
2
O
0.19 0.07 0.06 0.19 0.26 0.06 0.18 0.15
K
2
O
2.78 3.63 5.28 3.92 3.27 2.52 3.22 4.42
P
2
O
5
0.079
0.04 0.04 0.03 0.03 0.05 0.07 0.06
Cr
2
O
3
n.d. 0.006 0.005 n.d. 0.004 0.005 0.005 0.005
LOI
3.1
1.9
2.8
3.2
2.1
1.9
1.7
4.4
sum
100.03 99.91 99.81 99.89 99.93 99.87
99.9 99.88
Rb
ppm
119.7 108.0 232.9 140.4 115.7 91.3 150.4 137.9
Cs
6.9 4.1 12.3 4.3 10.9 11.8 9.3 16.0
Ba
196
130
209
142
110
395
275
189
Sc
6
7
10
3
3
3
4
4
Y
20.8 28.0 42.0 13.9 15.9 16.8 17.0 24.2
La
20.6 41.7 55.6 11.4 9.9 19.4 27.0 20.6
Ce
44.2 91.4
121.3 25.0 24.0 42.2 63.1 50.7
Pr
5.50
11.77
13.64 2.95 2.66 4.60 7.15 5.91
Nd
22.3 47.1 53.1 10.7 10.1 16.9 26.9 22.8
Sm
4.31 9.80 9.72 2.74 2.51 4.18 5.65 5.31
Eu
0.53 1.52 0.96 0.38 0.33 0.58 0.70 0.67
Gd
3.16 8.79 8.38 2.17 2.33 3.90 4.30 4.77
Tb
0.54 1.05 1.39 0.37 0.43 0.65 0.63 0.84
Dy
3.26 6.62 7.67 2.20 2.67 3.34 3.31 4.56
Ho
0.68 1.10 1.50 0.44 0.54 0.61 0.58 0.87
Er
1.96 2.99 4.17 1.28 1.48 1.67 1.48 2.21
Yb
2.00 2.82 3.93 1.45 1.49 1.37 1.28 2.01
Lu
0.32
0.43
0.57
0.20
0.19
0.19
0.17
0.26
Th
7.8
13.4
16.5 7.2 6.3
12.2 9.7 9.1
U
6.5 2.3 2.5 3.8 2.3 0.9 2.4 3.1
V
18
36
25
n.d.
n.d
11
17
n.d.
Co
22.5 3.1 5.0 1.2 3.5 4.0 3.5 2.4
Ni
16.7
21.7 4.9 1.9
19.7 9.3 6.5 1.9
Zr
96.1
378.8
344.1 43.1 56.5 73.5 79.8 63.6
Nb
7.6
13.0
18.5 8.9 6.0 8.6
10.4
14.2
Hf
3.1
10.5 9.9 2.3 2.7 2.5 3.1 2.5
Ta
0.9 1.0 1.3 1.1 0.9 0.6 0.9 1.5
Ga
14.7
12.7
10.9
12.8
15.6
10.9
12.8
15.6
Pb
1.8 1.4 0.9 2.3 0.5 0.7 0.6 0.6
Eu/Eu*
0.437 0.499 0.324 0.475 0.415 0.437 0.432 0.405
Fig. 3. Zr/Ti vs. Nb/Y diagram (Pearce 1996) corresponding to the
NGU Permian volcanic rocks. The zircon-dated samples are desig-
nated by bold bordered symbols.
!
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the widest range values of 22—60. Based on the FeO
tot
/MgO
ratios compared to the SiO
2
contents (Miyashiro 1974), the
studied andesite-rhyolite metavolcanites plot in the field of
calc-alkaline suite, with a slight tholeiite trend in basaltic
metaandesites. On the whole, they display chondrite-normal-
ized rare earth element patterns characterized by a variable
light rare earth element (LREE) enrichment and moderate to
pronounced negative Eu-anomalies, with no significant
heavy rare earth element (HREE) fractionation (Fig. 4). The
REE diagram shows apparently two different patterns:
Group I – is represented by the basaltic andesite-rhyolite
suite, with a slight enrichment in LREE (La
N
/Yb
N
= 4.51—9.99)
and Eu anomaly (Eu/Eu* ranging from 0.54 to 0.71), and
Group II – the rhyolite-dacite suite, with decreasing contents
of all the REEs compared to Group I and higher enrichment in
LREEs relative depletion of HREEs La
N
/Yb
N
= 14.33—9.61 and
a distinct Eu anomaly (Eu/Eu* ranging from 0.40 to 0.46).
Fractionation of plagioclases and titanomagnetites is responsi-
ble for the higher Eu and Ti anomalies and for depletion of Sr
and V in the Group II rocks. The high Rb/Sr ratios of the
Group II rhyolite-dacites, which are > 3, are also consistent
with the fractional crystallization of plagioclases.
In a primitive mantle-normalized multi-element variation
diagram (Fig. 5), the basic/intermediate and felsic metavol-
canites show similar enrichment and depletion trends. These
rocks are enriched in Rb, K, Th and U, and strongly depleted
in Ba, Sr, Nb, Ta and Ti. Compared to these, the basaltic
metaandesites are slightly enriched in Ti and depleted in U.
Enrichment in LILE and LREE with troughs at Ta-Nb and
Ti, is a distinctive feature considered typical of subduction-
Table 3: List of chemically analysed volcanic rock sample localities.
Sample
Lithostratigraphic unit
Sample locality
GPS coordinates
14 sm
Petrova hora Formation
1.1 km south from Jahodná, 572 m a.s.l.
N 48°46'113''
E 21°08'295''
15 sm
Novoveská Huta Formation
NW from Kamenný Hrb height, 530 m a.s.l.
N 48°45'590''
E 21°09'500''
25 sm
Novoveská Huta Formation
NW from Kamenný Hrb height, 530 m a.s.l.
N 48°45'590''
E 21°09'500''
19 sm
Petrova hora Formation
Čierna Hora height, NW from Dobšiná
N 48°85'836''
E 20°34'497''
20 sm
Petrova hora Formation
SE from Krompachy, 445 m a.s.l.
N 48°55'074''
E 20°53'818''
21 sm
Petrova hora Formation
SE from Krompachy, 445 m a.s.l.
N 48°55'074''
E 20°53'818''
33 sm
Petrova hora Formation
Kolínovce village, 388 m a.s.l.
N 48°55'688''
E 20°51'470''
34 sm
Petrova hora Formation
North from Richnava village, 372 m a.s.l.
N 48°55'799''
E 20°54'256''
36 sm
Petrova hora Formation
West from Jaklovce village, 396 m a.s.l.
N 48°52'408''
E 20°58'404''
39 sm
Petrova hora Formation
West from Jaklovce village, 361 m a.s.l.
N 48°52'160''
E 20°58'723''
41 sm
Petrova hora Formation
Southeast from Košická Belá, 390 m a.s.l.
N 48°47'740''
E 20°07'072''
GZ-32
Petrova hora Formation
East of Kuríšková height, 607 m a.s.l.
N 48°45'810”
E 21°09'000”
GZ-33
Novoveská Huta Formation
350 m NW from Kamenný Hrb height, 551 m a.s.l.
N 48°45'411”
E 21°09'746”
GZ-34
Novoveská Huta Formation
NW from Kamenný Hrb height, 603 m a.s.l.
N 48°45'393”
E 21°09'754”
Fig. 4. Chondrite-normalized REE patterns of the NGU Permian volcanic rocks. The chondrite normalizing values come from McDonough
& Sun (1995). A – Group I volcanics, B – Group II volcanics.
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related magma (Pearce 1983). Pearce et al. (1984) described
the specific patterns of rock chemical composition for within-
plate magmatites. That is exemplified by enrichment of Rb
relative to Nb and Ta, as well as Ce and Sm relative to adja-
cent elements (Fig. 5). According to Harris et al. (1983),
such selective enrichment can be attributed to crustal in-
volvement. However, unlike arc-type rocks, the whole stud-
ied NGU Permian volcanics display a distinct negative Ba
anomaly with respect to the adjacent Rb and Th. Such en-
richment of Rb and Th relative to Ba has also been observed
in the Permian high-K calc-alkaline magmatism in the
Southern Alps (Rottura et al. 1998), in the extension-related
Permian calc-alkaline andesites from the Pyrenees (Broutin
et al. 1994), in the Permian post-orogenic volcanites in the
Apuseni Mts (Nicolae et al. 2014), as well as in the Lower
Triassic alkaline rhyolites of the Silicum Unit in the Western
Carpathians (Uher et al. 2002). The observed enrichment of
Rb and Th relative to Ba cannot be considered in these sam-
ples as an effect due to the influence of hydrothermal fluids,
since Ba and Rb show a similar mobility and Th is consid-
ered immobile. Thus, the trough at Ba represents very likely a
primary magmatic feature. The large negative Ba anomaly
was also described by Pearce et al. (1984) for within-plate
granites situated in areas of attenuated continental lithosphere.
The whole group of the studied NGU Permian acid and in-
termediate metavolcanics has crustal values for both Nb/La
(0.44—0.27) and Nb/U (9.55—4.18) ratios, suggesting that
they are predominantly or wholly crustal melts. Magma deri-
Fig. 5. Multi-element variation diagram of the NGU Permian volcanic rocks. The primitive mantle normalizing values come from Sun &
McDonough (1989). A – Group I volcanics, B – Group II volcanics.
vation from continental crust or underplated crust is also in-
dicated by high Y/Nb ratios, ranging from 1.63 to 4.01. Ac-
cording to Eby (1992), these values are characteristic for the
A2-type of anorogenic magmatites, derived from partial
melting of continental crust or arc-type sources (Fig. 6A,B).
Y-Nb and Yb-Ta are the most effective elements for the
tectonic discrimination of granitic rocks as they seem to be
independent of alteration (Pearce et al. 1984). Fig. 7A,B
show simple projections in Y-Nb and Yb-Ta space. The meta-
rhyolite of Group I, associated with metaandesites, plots in
the within-plate granite field. The Group II metarhyodacites
overlap the volcanic-arc granite field. This scattered image
could indicate the post-collisional tectonic setting that can
result from variable mixture of mantle- and crust-derived
magma (Colman-Sadd 1982; Pearce et al. 1984). Thus, the
metarhyolite of Group I has all the classical characteristics of
A-type volcanism, including the high concentrations of alka-
lies, as well as incompatible elements, such as Nb, Y, Zr and
Th. Even associated metaandesites contain higher concentra-
tions of Nb, Y, Zr and Th than the metarhydacite of Group II
(Tables 1, 2). The metarhydacites of Group II have signifi-
cantly lower concentrations of REE, Y, Nb and Zr, and as a
result they plot in the volcanic arc field. Similar contrasting
types of silicic volcanic rocks were described by Christians-
en & McCurry (2008) from Cenozoic volcanism of the west-
ern Cordillera. According to their interpretation, they came
from different “mantle parents”, i) mantle wedge above sub-
duction zone (linkage to subduction heritage); ii) partial
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melting in/or above a mantle plume (continental rift and “hot-
spots”). The relationship to subduction processes for the
NGU Permian volcanics presumed Demko et al. (2007).
Zircon dating
Cathodoluminescence and optic imaging (Fig. 8) reveals
that zircons in both studied samples show prismatic and
dipyramidal shapes, obviously with well-developed growth
zoning and with less common sector zoning. Perfectly euhe-
dral zircon prisms without evidence of zoning were also ob-
served. Zircon crystals have a rather uniform internal texture,
characterized by a narrow fine oscillatory zoning only at
their margin. In some zircon crystals, the regular growth
zoning is interrupted by textural discontinuities along which
Fig. 6. Chemical characteristics of the NGU Permian volcanites according to Eby’s (1992) A-type granitoids subdivision. A – 10000Ga/Al vs.
Eu/Eu* discrimination diagram, B – Sc/Nb vs. Y/Nb discrimination diagram: A1 – granitoids from rift, plume and hot-spot environ-
ments, A2 – granitoids from post-collisional, post-orogenic and anorogenic environments.
Fig. 7. Nb-Y (A) and Ta-Yb (B) discrimination diagrams for NGU Permian metavolcanics after Pearce et al (1984). syn-COLG – syn-
collision granites, VAG – volcanic arc granites, WPG – within-plate granites, ORG – ocean ridge granites.
the original zoning is resorbed and succeeded by the new-
growth of zoned zircon rims. Textural discontinuities of the
magmatic zoning indicate resorption intervals during crystal
growths. In some cases, the oscillatory zoning is cut off by
areas of re-homogenization, recrystallization and local de-
velopment of convolute zoning.
Eleven spot analyses in the sample GZ-32 provided Permian
ages, in both the oscillatory – zoned rims and the internal
parts of crystals. Only one analysis indicates a Mississippian
age (332 ± 8 Ma). This age represents the maximum age and
suggests the involvement of material derived from the Mis-
sissippian magmatic rocks. The Permian ages display error
ellipses (2
σ) overlapping the concordia curve to a greater or
lesser extent (Fig. 9). Three results have not been included in
the average age calculation (spot analyses 4.1, 4.2, 7.1; Ta-
ble 4) due to the high U content or higher discordance. All
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the included results indicate U contents of 240—3323 ppm,
Th contents of 90—1203 ppm and Th/U ratios between
0.30—0.43. The considered 8 analyses yield
206
Pb/
238
U con-
cordant ages in the range of 262—276 Ma, with the
206
Pb/
238
U
concordia age of 269 ± 7 Ma (95% confidence, decay-con-
stant errors included; MSWD = 0.12; probability = 0.72). The
total – Pb/U (
238
U/
206
Pb—
207
Pb/
206
Pb) isochrones indicate the
concordia intercept at 271 ± 9 Ma (MSWD = 3.2) that coin-
cides approximately with the
206
Pb/
238
U concordia age (Fig. 9).
Ten zircon grains have been analysed from the sample
GZ-33. All the analysed spots were located in the uniform in-
ternal parts of the crystals, because the marginal rims of the
crystals are either very thin with a faint oscillatory zoning or
they are partly recrystallized and resorbed. Compared to the
sample GZ-32, zircons from the sample GZ-33 are signifi-
cantly richer in U and Th (Table 4). All ten measured grains
Fig. 8. Selected cathodoluminescence magmatic zircon images from the NGU Permian volcanic rocks with indication of the age data (in Ma)
based on
206
Pb/
238
U ratios.
Fig. 9. Concordia plot showing magmatic zircon ages from the sample GZ-32 and corresponding concordia intercept in the Terra-
Wasserburg diagram.
give
206
Pb/
238
U apparent ages, ranging between 248 and
255 Ma, which yield the concordia age of 251 ± 4 Ma (2
σ de-
cay-constant errors included, with MSWD = 0.74 and proba-
bility = 0.39). The concordia intercept at the Terra-Wasserburg
diagram confirms the same age of 252 ± 4 Ma (MSWD = 0.49;
Fig. 10).
Discussion
The
206
Pb/
238
U concordia age of 269 ± 7 Ma from the sam-
ple GZ-32 corresponds to the uppermost part of the Cisuralian,
and/or even straddling the Cisuralian/Guadalupian boundary
(Fig. 11). Compared to our previous zircon age data, it fits
well into the volcanites of the PHF from the vicinity of
Krompachy (272 ± 4 Ma and 275 ± 7 Ma for basaltic andesite
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Table 4:
U-Pb
(SHRIMP)
magmatic
zircon
ages
from
the
NGU
Permian
volcanic
rocks.
and rhyolite, respectively; Vozárová et al.
2012) indicating the Kungurian age. Gener-
ally, the new U-Pb zircon dating has a good
consistency with that. Nevertheless, zircons
from the sample GZ-32 show some recrystal-
lization features and modification in their tex-
ture (disruption of oscillatory zoning cutting
off by areas of re-homogenization, recrystal-
lization and local development of convolute
zoning). Even a slight modification of mag-
matic zircon crystals during late- and post-
magmatic processes could result in resetting
of U-Pb ages, (although, hardly distinguish-
able within error limits). Thus, this effect
could be a reason for the slight rejuvenation
and then the relatively younger ages in the
sample GZ-32 compared to previous results
from the Krompachy volcanics. Eventually,
all the obtained U-Pb ages are in the same
stratigraphic range, corresponding to the
Kungurian, and/or just near the boundary of
the Kungurian—Roadian. This time range de-
fines a dispersion of the main volcanic events
in the Permian of the NGU sedimentary ba-
sin. Similar U-Pb zircon ages were received
from the Southern Gemeric acid volcanites
(273.3 ± 2.8 Ma and 275.3 ± 2.9 Ma, respec-
tively; Vozárová et al. 2009b), as well as
from the rhyolite-dacites of the Northern
Veporic Unit (273 ± 6 Ma and 279 ± 4 Ma;
Vozárová et al. 2010) and the Gemeric gran-
ites (Finger & Broska 1999; Kohút & Stein
2005; Radvanec et al. 2009). Analogous zir-
con ages, ranging from 279.6 ± 1.1 Ma to
274.1 ± 1.6 Ma, were reported by Bargossi et
al. (2004) from the Bolzano Volcanic Com-
plex in the Southern Alps. A corresponding
sequence comprising rhyodacites and their
ignimbrites is widespread at the top of the
Cisuralian succession in the Eastern Alps
that also correlates with the Bolzano Volca-
nic Complex (Krainer in McCann et al. 2008).
However, the detrital zircon age spectra
from the two samples of the NGU Permian
sandstones (both PHF and NHF) also indi-
cate the presence of older magmatic events
in the depositional area, corresponding to the
Sakmarian and to the Artinskian (concordia
ages 281 ± 7 Ma and 292 ± 6 Ma; Vozárová et
al. 2013). No doubt, these zircon grains were
redeposited as clastic detritus from the co-
eval volcanic centers into the sedimentary
basin and they mixed with spatially wide-
spread non-volcanic detritus, and even could
have been reworked in the younger Permian
sediments. Thus, the NGU Permian bulk ig-
neous activity, as in many other areas of the
Central and Southern European Variscides
(Rottura et al. 1998; Vozárová et al. 2010;
Errors
are
1-sigma;
Pb
c
and
Pb*
indicate
the
common
and
radiogenic
portions,
respectively.
Error
in
Standard
calibration
was
0.73 %
(not
included
in
above
errors
but
required
when
comparing
data
from
different
m
ounts).
(1)
Common
Pb
corrected
using
measured
204
Pb.
Disc.
=
diskordia.
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Fig. 10. Concordia plot showing magmatic zircon ages from the sample GZ-33 and corresponding concordia intercept at the Terra-Wasserburg
diagram.
Fig. 11. The SHRIMP zircon age timescale of the NGU Permian
volcanic rocks. Column A – age results from the present paper,
column B – magmatic zircon ages published in Vozárová et al.
(2012), column C – zircon ages derived from detrital zircon as-
semblages of the Petrova hora and Novoveská Huta Formations
(taken from Vozárová et al. 2013).
Nicolae et al. 2014 and references therein), took place mainly
throughout the Cisuralian. It seems not to function later than
the early Guadalupian (Roadian), that predates the Illawara
Reversal geomagnetic event (IR ca. 265 Ma; Menning
2001). The only exceptions in the Western Carpathians are
the basaltic volcanic suite of the 2
nd
eruption phase in the
Hronic Unit that is located over the IR (Vozárová & Túnyi
2003) and silicic volcanites in the Bôrka Nappe (260 Ma;
Vozárová et al. 2012). The question remains, if the NGU
Permian volcanism represents one long-lasting episode or
two independent volcanic events. The Cisuralian bulk volca-
nic activity was probably split mostly into two independent
events, the first extending throughout the Sakmarian and the
second one during the Kungurian. Of course, this assump-
tion should be confirmed by further precise zircon dating.
Sample GZ-33 shows a significantly diverse age (Fig. 10,
Table 4). The apparent
206
Pb/
238
U ages vary between 248 and
255 Ma, which yield the concordia age of 251 ± 4 Ma. Com-
pared to the age results of sample GZ-32, and the samples
dated previously from the NGU Permian volcanites
(Vozárová et al. 2012), the sample GZ-33
206
Pb/
238
U zircon
age is significantly younger. The difference between these two
data groups is less than ca. 20 Ma. The detected U-Pb zircon
ages document, for the first time, the boundary Permian/Trias-
sic volcanism in the Western Carpathians. According to the
International Stratigraphic Chart 2014 (International Sub-
comission on Stratigraphy, 2014; updated according to Cohen
et al. 2013), the boundary between the Permian and Triassic
systems is established at 252.17 ± 0.06 Ma.
The NGU Permian-Triassic volcanic event seems to be ap-
proximately coeval with the sedimentation of the NHF evapor-
ite member that is correlated with the Zechstein (in the sense of
Regional Stratigraphic Scale, Stratigraphic Table of Germany
Compact 2012) based on the S and O isotopes (Kantor et al. in
Vozárová 1997). The polymict conglomerates (the Strážany
Beds according to Mihát in Rojkovič & Mihát 1991) that under-
lie this evaporitic lithofacies, contain fragments of volcanites,
which were redeposited from the Cisuralian volcanic suite.
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Occurrences of evaporites, associated with fine-grained
sandstones, shales and dolomites have been recognized in
the boreholes from the vicinity of the village of Košická
Belá, north of the Permian-Triassic boundary volcanic hori-
zon. These sediments fall within the youngest formation of
the Permian sequence around Košice and Košická Belá and
have been correlated with the evaporite horizon in the area of
Novoveská Huta (Václav & Vozárová 1978), and later affili-
ated to the NHF (Bajaník et al. 1981). As the radiometric age
data from the Permian volcanites of the Košice—Košická Belá
area are generally missing, all these volcanic rocks were as-
signed to the PHF. The presented zircon age data enable us
to separate a part of these volcanic rocks from the PHF and
to synchronize them with the NHF (Fig. 12).
On the account of that, the stratigraphic gap from the end
of Cisuralian eventually from the mid-Guadalupian to the
Lopingian, is supposed to be trustworthy. The major strati-
graphic gap and viable break of sedimentation within the
NGU Permian sequence were probably caused by a tectonic
pulse that most likely induced extensional faulting and uplift
connected with strike-slip movements and erosion at least in
some places. This tectonic event could have been related to
the so-called “Mid-Permian Episode” of Deroin & Bonin
(2003), connected with the transformation of strike-slip to an
extensional tectonic regime. A similar stratigraphic gap and
geodynamic changes were described in the Eastern and South-
ern Alps as well as in the wide peri-Mediterranean realm
(Krainer 1993; Cassinis et al. 2012 and references therein) that
was reflected in the evolution of two major tectono-sedi-
mentary cycles. Cassinis et al. (2012) considered this strati-
graphic gap to be synchronous with the geomagnetic IR event
(Menning 1995, 2001; Steiner 2006) that has been postulated
by Isozaki (2009) as the trigger agent for the Pangea breakup.
However, the
206
Pb/
238
U zircon ages in the sample GZ-33
undoubtedly document a specific stage of volcanic activity
that is different from the Cisuralian one. Its discrepancy is
highlighted by differences in time and partly also in geo-
Fig. 12. Schematic geological map of the NGU Permian sequence
from the vicinity of Košice—Košická Belá, modified from Mihái
(1990 in Rojkovič & Mihái 1991).
chemistry. As the dacites represented by the sample GZ-32
have prevailing K
2
O over Na
2
O (5.16 wt. % vs. 0.60 wt. %),
they may indicate the high-K calc-alkaline volcanic series. On
the contrary, in the samples GZ-33 and GZ-34 (Tables 1, 2), a
significant increase of the Na
2
O (4.15 and 7.14 wt. %) over
K
2
O (3.02 vs. 0.42 wt. %) has been determined. However, all
the analysed samples show the same trend of enrichment in
LREE as well as in incompatible elements such as U, Th, Ta
and Nb in comparison with the moderately incompatible Ti
and HREE. Similarly, the ratios Nb/La and Nb/U that serve as
magma genesis indicators have the same values, for Nb/La in
the range of 0.27 to 0.33 and for Nb/U ranging from 5.2 to 4.2.
These low ratio values are close to the continental crust data
and are characteristic for crustal melting (Nb/La = 0.71 and
Nb/U = 9.7 for continental crust calculated by Rudnick &
Fountain 1995).
In the Western Carpathians, Lower to Middle Triassic high-K
rhyolites have been described from the Silicic Unit (Uher et al.
2002). They were interpreted by the authors as genetically
connected with the early Alpine rifting. Similarly, the U-Pb
zircon age of 233 ± 4 Ma (Putiš et al. 2001) from the plagio-
granite-aplitic vein bodies cutting the Layered Amphibolite
Complex in the Veporic crystalline basement was interpreted.
On the contrary, the monazite ages from the geologically
equivalent rhyolite body (the Silicic Unit), at Gregová near
Telgárt village, confirmed the Middle/Upper Permian age of
263 ± 3.5 Ma (Demko & Hraško 2013). The intermediate to
basic Middle Triassic anorogenic volcanism was described
from the wide area of the Transdanubia, Bukkia and Adria-
Dinaria terranes (Kovács et al. 2010 and references therein).
The acid to intermediate volcanism, as it has been already
mentioned, is dominant in the Cisuralian with the exception of
the Ligurian Alps, where this volcanism is situated above the
IR horizon (Dallagiovanna et al. 2009; Cassinis et al. 2012 and
references therein), but not at the Permian/Triassic boundary.
Although the NGU Permian volcanites show some geo-
chemical features similar to arc-related suites (enrichment in
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LILE and LREE with troughs at Ta-Nb and Ti; Pearce 1983),
the paleogeographic reconstruction and geological and tec-
tonic evidence (Bajaník et al. 1984; Novotný & Mihá] 1987;
Vozárová & Vozár 1988; Rojkovič & Mihá] 1991; Vozárová
1996), do not support any spatial and temporal connection
with subduction processes. This volcanism post-dates the
355 peak of the Variscan metamorphism in the NGU realm
(Putiš et al. 2009; Vozárová et al. 2013), as well as the late
Bashkirian-Moscovian uplift of the metamorphic nappes in
the NGU Variscan orogenic belt (Vozárová 1973, 1996;
Vozárová et al. 2013 and references therein). It is post-colli-
sional with respect to the Late Devonian-Mississippian colli-
sion, that led to the accretion of the NGU orogenic belt to the
Prototatricum crust (the term Prototatricum is coined by
Broska et al. 2013 for the common Variscan basement of the
Tatricum and the Veporicum Units) which was the part of
the Galatian Superterrane (von Raumer & Stampfli 2008;
von Raumer et al. 2009; Stampfli et al. 2011), with the oce-
anic crust of the Prototethys. Radvanec et al. (2009) argued
that the crustal extension above the Late Variscan subduc-
tion zone was the origin of the Gemeric granites, as well as
the Permian volcanics.
In the Th/Yb vs. Nb/Yb diagram (Fig. 13), all the NGU Per-
mian samples are plotted outside the diagonal MORB-OIB
array, on a vector at a steep angle but closer to E-MORB for
Group I, and may be related to the variable fractionation pro-
cesses and variable crustal contamination (Pearce 2008).
Group I, represented by the basaltic andesite-rhyolite suite,
shows depletion in Th and Nb compared to rhyolite-dacite
suite of Group II. These data suggest that the Group I volca-
nic rocks were derived by partial melting of enriched litho-
sphere mantle, modified by subducted slab-derived fluids.
The rhyolite-dacite suite magma of Group II was probably
generated by partial melting of newly accreted crust.
Conclusions
1. The new
206
U/
238
Pb zircon ages confirm the dominant
Kungurian volcanic event in the NGU Permian sedimentary
basin. Simultaneously, Permian-Triassic boundary volcanism
at 251 ± 4 Ma is indicated for the first time;
2. The NGU Permian volcanites have petrological and
geochemical characteristics similar to those of a subduction
related calc-alkaline suite. However, geological and tectonic
evidence points to an intracontinental extensional regime,
associated with the Late Paleozoic dextral transtensional tec-
tonics caused by the relative motion of Gondwana and
Laurasia (Vai 1991, 2003; Ziegler 1993; Torsvik & Cocks
2004; Muttoni et al. 2009). The NGU volcanic rocks may
have been formed by an extensive crustal contamination of
basaltic-intermediate magma (Group I) derived from an en-
riched lithospheric mantle source and by partial melting of
newly accreted crust (Group II);
3. The NGU Permian volcanic activity was associated
with the polyphase extensional tectonic regime. Based on the
U-Pb zircon ages, the bulk of the NGU Permian activity oc-
curred during the Cisuralian, mostly during the Sakmarian
and the Kungurian. Both were related to the post-orogenic
transpression/transtension and extensional tectonic move-
ments that reflect the consolidation of the Variscan orogenic
belt. The last volcanic phase was linked with extension at the
Permian-Triassic boundary that was in the NGU realm in
connection with the beginning of the Alpine orogenic cycle.
Acknowledgments: The financial support of the Slovak Re-
search and Development Support Agency (Project ID:
APVV-0546-11) is gratefully acknowledged. The authors
are highly grateful to Alexander Larionov for thorough read-
ing and improving remarks and comments. We would like to
express our thanks to Prof. F. Neubauer and Assoc. Prof. Peter
Ivan for their constructive suggestions in the earlier version
of the manuscript.
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