GEOLOGICA CARPATHICA
, APRIL 2018, 69, 2, 187–198
doi: 10.1515/geoca-2018-0011
www.geologicacarpathica.com
Permian A-type rhyolites of the Muráň Nappe,
Inner Western Carpathians, Slovakia:
in-situ zircon U–Pb SIMS ages and tectonic setting
MARTIN ONDREJKA
1,
, XIAN-HUA LI
2
, RASTISLAV VOJTKO
3
, MARIÁN PUTIŠ
1
,
PAVEL UHER
1
and TOMÁŠ SOBOCKÝ
1
1
Department of Mineralogy and Petrology, Faculty of Natural Sciences, Comenius University in Bratislava, Mlynská dolina,
Ilkovičova 6, 842 15 Bratislava, Slovakia;
martin.ondrejka@uniba.sk
2
State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China
3
Department of Geology and Palaeontology, Faculty of Natural Sciences, Comenius University in Bratislava,
Mlynská dolina, Ilkovičova 6, 842 15 Bratislava, Slovakia
(Manuscript received November 6, 2017; accepted in revised form February 15, 2018)
Abstract: Three representative A-type rhyolitic rock samples from the Muráň Nappe of the inferred Silicic Unit of
the Inner Western Carpathians (Slovakia) were dated using the high-precision SIMS U–Pb isotope technique on zircons.
The geochronological data presented in this paper is the first in-situ isotopic dating of these volcanic rocks. Oscillatory
zoned zircon crystals mostly revealed concordant Permian (Guadalupian) ages: 266.6 ± 2.4 Ma in Tisovec-Rejkovo
(TIS-1), 263.3 ± 1.9 Ma in Telgárt-Gregová Hill (TEL-1) and 269.5 ± 1.8 Ma in Veľká Stožka-Dudlavka (SD-2) rhyolites.
The results indicate that the formation of A-type rhyolites and their plutonic equivalents are connected to magmatic
activity during the Permian extensional tectonics and most likely related to the Pangea supercontinent break-up.
Keywords: Permian volcanism, Western Carpathians, Muráň Nappe, A-type rhyolites, zircon, SIMS U–Pb age.
Introduction
Numerous occurrences of acid volcanic rocks, mainly rhyo-
lites in Permian to Lower Triassic siliciclastic to carbonate
sequences of the inferred Silicic Unit Muráň and Drienok
nappes have been reported by many authors (e.g., Stur 1868;
Oppenheimer 1931; Grenar & Kotásek 1956; Zorkovský
1959 a, b; Losert 1963; Slavkay 1965, 1981; Klinec 1976;
Hovorka & Spišiak 1988; Uher et al. 2002 a, b; Ondrejka et al.
2007, 2015; Demko & Hraško 2013). The (trachy)andesite–
trachyte–rhyolite lava and pyroclastic sequences as belonging
to the K-alkalic association (according to de La Roche et al.
1980 classification) were characterised in the PO-1 borehole
near Poniky village in the Drienok Nappe (Slavkay 1965,
1981). The sequence was named the Skálie Formation and it
corre lates with the Lower Triassic volcanic suite of the Bükk
Unit in Hungary (Hovorka & Spišiak 1988). The major and
trace element geochemical and mineralogical characteristics
of these volcanic rocks (Uher et al. 2002 b) are compatible
with analogous occurrences of post-Variscan anorogenic
A-type magmatic rocks in the Alpine-Carpathian belt (e.g.,
Bonin 1990; Beltrán-Triviño et al. 2016).
The lack of convincing radiometric dates has confused
previous authors about the stratigraphic position of these
rhyolites and their inferred Early Triassic age (Biely 1956;
Slavkay 1965, 1981; Mello et al. 2000 b; Uher et al. 2002 a, b;
Ondrejka et al. 2015). However, the age of these volcanic
rocks was deduced only from their close geological position to
adjacent Triassic sediments (Klinec 1976; Slavkay 1981;
Mello et al. 2000 a, b). Determination of the exact age of these
volcanites resulted in EPMA monazite dating of the Gregová
rhyolite body which gave a Guadalupian age of 263 ± 3.5 Ma
(Demko & Hraško 2013). This geochronological data was
supported by comprehensive petrographical, lithofacial, and
volcanological study which reported the close volcanics rela-
tionship to Permian sedimentary succession upwards followed
by Triassic sediments (Demko & Hraško 2013). However,
a precise geochronological solution is required to place these
volcanites in stratigraphic successions of the inferred Silicic
Unit Muráň Nappe in the southern part of the Inner Western
Carpathians. The aim of this paper is to yield accurate radio-
metric ages for these acid volcanic rocks by in-situ zircon
U–Pb SIMS isotopic dating. We selected three typical occur-
rences of the rhyolites from Muráň Nappe: Tisovec-Rejkovo,
Veľká Stožka-Dudlavka, and Telgárt-Gregová Hill for this
dating (Fig. 1).
Geological setting, mineral composition,
geochemistry and petrology of A-type rhyolites
The Silicic Unit (e.g., Plašienka et al. 1997) includes the
struc
turally highest, non-metamorphosed nappe stack
restricted to the Vepor-Gemer Belt of the Inner Western
Carpathians and to the Slovak-Aggtelek Karst to the south.
(i.e. Drienok, Muráň, Vernár, Stratená, Silica, Szőlősardó,
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GEOLOGICA CARPATHICA
, 2018, 69, 2, 187–198
and Bódva nappes). Lithostratigraphy establishes Late Permian
to Late Jurassic sedimentary successions dominated by exten-
sive Middle to Late Triassic platform-type carbonates, and
the unit is facially analogous to the Schneeberg and Mürzalpe
nappes of the Upper Tirolic and/or Juvavic nappes of the
Northern Calcareous Alps (Mello et al. 1997).
The original sedimentary position of the Silicic Unit is not
well constrained. Facially, it could be placed on the northern
passive margin of the Meliata (Neotethys) Ocean (Haas et al.
1995) but the structural position on the top of the nappe stack
would infer origin from the southern margin of the Ocean
(as in Hók et al. 1995, 2014; Putiš et al. 2014; Lačný et al.
2016; Plašienka et al. 2016).
The lower part of the Silicic Unit is composed of the Werfen
Formation. This ranges from tens to hundreds of metres thick
sedimentary succession of continental to shallow marine
Fig. 1. Position of investigated rhyolites of the Muráň Nappe in the Inner Western Carpathians: A — Tisovec-Rejkovo (TIS-1), N 48°40’7.89”,
E 19°55’28.96”; B — Veľká Stožka-Dudlavka (SD-2), N 48°46’9.42”, E 19°56’32.47”; C — Telgárt-Gregová Hill (TEL-1), N 48°51’21.41”,
E 20°12’16.13”: The geological maps are modified after Klinec (1976).
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PERMIAN A-TYPE RHYOLITES OF THE MURÁŇ NAPPE, INNER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2018, 69, 2, 187–198
deposits, mainly shales to sandstones with marlstones, lime-
stones and a siliciclastic admixture of Late Permian to Early
Triassic age (Bystrický 1964; Slavkay 1965; Klinec 1976;
Biely et al. 1992, 1997; Mello et al. 2000 a, b; Vojtko 2000).
From this group of nappe stack, the Muráň, Vernár, and Drienok
nappes contain the rhyolite bodies in the lower portion of
the formation (Fig. 2; Bódvaszilas Member; Hips 1996).
The A-type rhyolitic rocks have the common features of
acid volcanics. The texture is commonly porphyric with
a microfelsitic to felsitic groundmass. Fluidal texture also
occurs in some places. Phenocrysts, 0.5–4 mm in size, are
represented by euhedral mesoperthitic alkali feldspars (Fig. 3a)
and corroded ß-quartz (Fig. 3b). The feldspars are commonly
replaced by post-magmatic chessboard albite or fine-grained
aggregates of white mica (Uher et al. 2002b; Ondrejka et al.
2007). The groundmass consists of a very fine-grained aggre-
gate of quartz, alkali feldspar, white mica, hematite pigment,
and occasionally biotite, chlorite, and accessory zircon,
monazite-(Ce), xenotime- (Y), rutile, ilmenite, magnetite,
hematite, and barite (Uher et al. 2002b; Ondrejka et al. 2015)
(Fig. 3c). Moreover, the rhyolite body at Tisovec-Rejkovo
contains a unique REE–Y–(Th)–P–As–(Si)–(Nb)–(S) acces-
sory assemblage comprising REE arsenate-phosphate-silicate
solid solutions, REE carbonates and rarely cerianite-(Ce)
(Ondrejka et al. 2007).
All studied rhyolites are rich in Si and especially K, and
depleted in Ti, Mg, Ca, Na, and P (Uher et al. 2002 a, b;
Ondrejka et al. 2007). Despite the relatively low Al contents
due to depletion in Ca and Na, the rhyolites are peraluminous
with A/CNK = 1.15 to 1.7. High Si contents connected with
low Mg and Ca resulted in anomalously high R1 parameter
and very low R2 (after Batchelor & Bowden 1985) with
a trend concordant with anorogenic magmatic suites (Uher et
al. 2002 b). The rhyolites trace element geochemistry has slight
enrichment in Rb, Zr, Y and REE, depletion in Sr, Ba and V, as
well as elevated Rb/Sr and Ga/Al ratios (Uher et al. 2002 b)
which are typical for alkali-rich post-orogenic and anorogenic
Si-rich magmatic suites of A-type affinity (Whalen et al.
1987). The A-type tendency is also evident in chondrite-
normalised REE distribution patterns with pronounced nega-
tive Eu-anomaly and slightly enriched LREEs (Uher et al.
2002 b; Ondrejka 2004).
Zircon typology of the rhyolites shows dominant high alka-
line and high temperature (800 –900 ± 50 °C) types and sub-
types (Fig. 3d,e; Uher et al. 2002 b; Ondrejka et al. 2015)
which are characteristic for anorogenic alkaline magmatic
Fig. 2. Simplified Permian to Triassic lithostratigraphic column of the Vernár Nappe and Muráň Nappe.
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ONDREJKA , LI , VOJTKO, PUTIŠ, UHER and SOBOCKÝ
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, 2018, 69, 2, 187–198
suites (Pupin 1980). These results correspond with the zircon
saturation temperatures (T
Zr
) of the rhyolites, calculated from
bulk-rock chemical composition (Watson & Harrison 1983),
where T
Zr
= 820 – 895 °C (Uher et al. 2002 b; Ondrejka et al.
2015). The study of Fe –Ti oxide mineral assemblage reveals
late magmatic to (sub)solidus evolution of the rhyolites, with
estimated equilibrium temperatures from ~ 750 to ~ 400 °C and
oxygen fugacity values approaching the NiNiO buffer from
– 0.76 Δlog f O
2
(~ 626 °C) to 1.53 Δlog f O
2
(~655 °C) (Ondrejka
et al. 2015).
Analytical methods
Zircon crystals were extracted using standard density and
magnetic separation techniques. Zircons and zircon U–Pb age
standards were mounted in 2.5 cm diameter epoxy polished to
expose the crystal interiors for analysis. Zircon crystals were
documented with transmitted and reflected light microphoto-
graphs, followed by cathodoluminescence (CL) imaging under
a field emission scanning electron microscope equipped with
Gatan MonoCL4 detector at the Institute of Geology and
Geophysics, Chinese Academy of Sciences (IGG-CAS) in
Beijing. After imaging, the zircon mount was coated with high
purity gold to reach < 20 Ω resistance prior to SIMS analysis.
Measurement of U, Th, and Pb isotopes was conducted
using a Cameca IMS-1280HR SIMS at the Institute of Geology
and Geophysics, Chinese Academy of Sciences in Beijing.
The instrument description and analytical procedure follow Li
et al. (2009), and we give only a brief summary. The primary
O
2
−
ion beam spot is approximately 20 × 30 μm in size. Positive
secondary ions were extracted with a 10 kV potential. A 60 eV
energy window was used in secondary ion beam optics with
mass resolution of approximately 5400 (at 10 % peak height)
to separate Pb
+
peaks from isobaric interferences. A single
electron multiplier was then used in ion-counting mode to
measure secondary ion beam intensities by peak jumping
mode. Each measurement consists of 7 cycles. The Pb/U
calibration was performed relative to the Plešovice zircon
standard (
206
Pb /
238
U age = 337.13 ± 0.37 Ma; Sláma et al. 2008);
U and Th concentrations were calibrated against zircon stan-
dard 91500 (Th = 29 ppm, and U = 81 ppm, Wiedenbeck et al.
Fig. 3. Microphotographs, BSE and SEM images showing textural aspects and mineral composition of A-type rhyolites of the Muráň Nappe:
a — phenocryst of euhedral chessboard albite (Fs) and fine-grained aggregates of white mica (X polaroids); b — phenocrysts of corroded
ß-quartz (II polaroids); c — zircon (Zrn) and monazite-(Ce) (Mnz) enclosed in Fe-Ti oxide trellis aggregates represented by magnetite, ilmenite
(Mt/Ilm) and rutile, hematite (Rt/Hem); d — zircon crystal of D type morphology; e — zircon crystal of P
5
subtype morphology.
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PERMIAN A-TYPE RHYOLITES OF THE MURÁŇ NAPPE, INNER WESTERN CARPATHIANS
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, 2018, 69, 2, 187–198
1995). A long-term uncertainty of 1.5 % (1s RSD) for
206
Pb /
238
U
measurements of the standard zircons was propagated to the
unknowns (Li et al. 2010), although the measured
206
Pb /
238
U
error in a specific session is generally ≤ 1% (1σ RSD).
Measured compositions were corrected for common Pb
using non-radiogenic
204
Pb. Corrections are sufficiently small
to be insensitive to the choice of common Pb composition,
and the average of present-day crustal composition (Stacey
& Kramers 1975) is used for the common Pb; assuming
that the common Pb is largely surface contamination intro-
duced in sample preparation. Data reduction was performed
by Isoplot/Ex version 2.49 program (Ludwig 2001).
Uncertainties on individual analyses in data tables are reported
at 1σ level, and Concordia U–Pb ages are quoted with
95 % confidence interval except where otherwise noted.
The Qinghu (China) zircon standard and samples were alter-
nately analysed as unknowns in order to monitor the external
uncertainties of SIMS U–Pb zircon dating calibrated against
the Plešovice standard. Twenty-two Qinghu zircon measure-
ments yielded concordia age of 160 ± 1 Ma which is identical
within error to the 159.5 ± 0.2 Ma recommended value (Li et
al. 2013).
Results
Zircon descriptions
Zircon crystals were separated from the A-type rhyolites
from Tisovec (TIS-1 sample), Telgárt (TEL-1 sample), and
Veľká Stožka (SD-2 sample). The highest quality zircon
crystals in all samples were selected for measurement to avoid
fractures and mineral inclusions. The apparent zircon mor-
phology ranges from euhedral and long-prismatic to sub-
hedral, stubby grains. Among them, the euhedral crystals are
the most common. Some zircons have slightly resorbed shapes
with varying degree of crystal-edge rounding. Zircons crystals
are transparent, mostly 100 –200 µm in length with length /
width ratios of ~ 1.5:1 to ~ 3:1. While magmatic regular fine
oscillatory and sector zoning are common features of the
investigated zircon crystals, irregular (subsolidus?) domains
are also visible in CL imaging (Fig. 4).
SIMS zircon U–Pb ages
A total of 58 spot analyses were performed on zircon crystals
from samples TIS-1, TEL-1 and SD-2. The zircons reveal
variable concentrations of uranium (~ 40 to 930 ppm) and
thorium (~15 to 1220 ppm) which give a relatively wide
Th/U ratio between 0.05 and 2.33 for all three samples
(Tables 1 to 3). Values for f
206
(the proportion of common
206
Pb
in total measured
206
Pb) are in the range of 0.09 –3.19 %
(TIS-1, Table 1), 0.24–1.25 % (TEL-1, Table 2) and 0.04–
1.66 % (SD-2, Table 3).
A total of 19 spot analyses were obtained from the Tisovec-
Rejkovo rhyolite, TIS-1 sample (Table 1). Apart from a single
zircon crystal (spot TIS-1-1) which shows a different mor-
phology (S-subtypes), the remaining 18 zircon crystals exhibit
D or P
4-5
morphology (according to typology of Pupin 1980)
(Fig. 4). Their U–Pb isotope analyses are concordant within
analytical errors; yielding a concordia age of 266.6 ± 2.4 Ma
(MSWD of concordance = 1.3) (Fig. 5). Spot TIS-1-1 gives
a clearly older age of 462.7 ± 6.6 Ma (1σ) which is interpreted
as an inherited xenocryst.
A total of 19 spot analyses were obtained from the Telgárt-
Gregová Hill rhyolite, TEL-1 sample (Table 2). One analysis
(spot TEL-1-5) yields a clearly older date of 781.2 ± 11.6 Ma
(1σ) than the majority of the population. This zircon has
unambiguously resorbed shape with irregular zoning under
CL, thus indicating a potential inherited xenocryst in origin.
The remaining 18 zircons are mostly euhedral crystals with
concentric zoning (Fig. 4). They give concordant U–Pb
results within analytical errors; yielding a concordia age of
263.3 ± 1.9 Ma (MSWD of concordance = 0.16) (Fig. 6).
A total of 20 spot analyses were conducted for the Veľká
Stožka-Dudlavka, SD-2 sample (Table 3). One analysis
(spot SD-2-2) gives a clearly younger date of 239.0 ± 3.5 Ma
(1σ) than others, possibly due to partial loss of radiogenic Pb.
The remaining 19 analyses are concordant within analytical
errors, yielding a concordia age of 269.5 ± 1.8 Ma (MSWD of
concordance = 0.19) (Fig. 7).
Discussion and conclusion
Acid volcanic rocks of the inferred Silicic Unit Muráň
Nappe in the Inner Western Carpathians were investigated
mainly from the view-point of their stratigraphic position and
determination of their petrographic composition (Zorkovský
1959 a, b; Slavkay 1965, 1981) and mineralogical–geochemical
characteristics (Uher et al. 2002 a, b; Ondrejka et al. 2007, 2015).
Lithological and stratigraphic correlations without radiometric
data prompted previous authors to deem the rhyolites of
the Silicic Unit as Early Triassic (Biely 1956; Slavkay 1965,
1981; Mello et al. 2000 b; Uher et al. 2002 a, b; Ondrejka et
al. 2015).
The magmatic crystallisation ages of ca. 270 –263 Ma
presented in this paper are the first in-situ isotopic ages of
these volcanic rocks constrained by the U–Pb SIMS method
on zircon. However, already the first preliminary geochrono-
logical results indicated a Permian age for the rhyolites in
question. These were obtained from the Poniky-Drienok
(261 ± 15 Ma) and Veľká Stožka (258 ± 12 Ma) rhyolite bodies
by the in-situ EPMA U–Th–Pb method on monazite (Ondrejka
2004). The ages are relatively imprecise due to low Th,
U contents measured by EPMA and the restricted number of
analytical spots (12 and 15 respectively) which resulted in
relatively large 2σ errors. Moreover, recent monazite EPMA
chemical dating from the Telgárt-Gregová Hill rhyolite body
gave a more precise Permian age (Guadalupian) of 263 ± 3.5 Ma
(Demko & Hraško 2013) which is in good agreement with our
presented SIMS U–Pb ages.
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ONDREJKA , LI , VOJTKO, PUTIŠ, UHER and SOBOCKÝ
GEOLOGICA CARPATHICA
, 2018, 69, 2, 187–198
Fig. 4. CL images of zircons from the A-type rhyolite from Muráň Nappe with illustrated analytical spots and corresponding
206
Pb /
238
U
age values.
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PERMIAN A-TYPE RHYOLITES OF THE MURÁŇ NAPPE, INNER WESTERN CARPATHIANS
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Analogous zircon U–Pb SIMS ages of ca. 270 to 260 Ma
were determined from the following locations; a rhyolite lava
flow in Permian siliciclastics and rhyodacite dyke in crystal-
line basement micaschist-gneisses of the Infratatric Unit in
the Považský Inovec Mts. (~ 267–262 Ma; Putiš et al. 2016),
a quartz-bearing, magmatically mixed and/or contaminated
volcanic dykes of alkaline basalt in the Tatric Unit of
the Považský Inovec Mts. (~ 260 Ma; Pelech et al. 2017),
the A-type Turčok metagranite (~ 263 Ma; Radvanec et al.
2009) and rare metal S-type granites in the Gemeric Unit
~ 275 –250 Ma (Finger & Broska 1999; Kohút & Stein 2005;
Radvanec et al. 2009). Permian ages of acid magmatism were
also documented in the Northern Veporic Unit, including
the eastern part of the Nízke Tatry Mts. (Kotov et al. 1996;
Bezák et al. 2008; Vozárová et al. 2016). Very similar age
intervals (~ 275 –255 Ma) were also obtained from volcanic
sample/spot
U
Th
Pb
Th/U
f
206
207
Pb/
235
U
±σ
206
Pb/
238
U
±σ
206
Pb/
238
U
±σ
207
Pb/
235
U
±σ
(ppm)
(ppm)
(ppm)
(%)
(%)
(%)
age (Ma)
(Ma)
age (Ma)
(Ma)
TIS-1/1
266.5
14.2
20.8
0.053
0.09
0.57731
2.17
0.0727
1.50
452.2
6.6
462.7
8.1
TIS-1/2
620.3
412.6
33.0
0.665
0.18
0.30316
1.69
0.0422
1.50
266.3
3.9
268.9
4.0
TIS-1/3
474.0
274.8
25.1
0.580
0.26
0.30312
1.77
0.0429
1.50
271.0
4.0
268.8
4.2
TIS-1/4
557.9
427.2
28.8
0.766
3.19
0.29134
4.14
0.0410
1.71
259.2
4.3
259.6
9.5
TIS-1/5
740.2
434.9
39.0
0.588
0.41
0.30447
1.67
0.0425
1.50
268.4
3.9
269.9
4.0
TIS-1/6
548.7
326.2
28.5
0.595
0.18
0.29541
1.87
0.0420
1.51
265.3
3.9
262.8
4.3
TIS-1/7
428.2
235.0
22.4
0.549
0.34
0.30453
1.78
0.0429
1.50
270.7
4.0
269.9
4.2
TIS-1/8
432.2
351.8
23.8
0.814
0.40
0.29153
2.30
0.0422
1.50
266.5
3.9
259.8
5.3
TIS-1/9
933.0
978.4
54.1
1.049
0.35
0.29292
1.90
0.0421
1.50
265.6
3.9
260.9
4.4
TIS-1/10
492.6
293.1
26.2
0.595
0.10
0.30421
1.81
0.0429
1.50
270.7
4.0
269.7
4.3
TIS-1/11
902.3
892.9
53.0
0.990
0.36
0.30256
2.29
0.0430
1.50
271.6
4.0
268.4
5.4
TIS-1/12
466.5
279.9
24.2
0.600
0.20
0.29882
1.77
0.0419
1.50
264.3
3.9
265.5
4.1
TIS-1/13
426.1
255.3
21.7
0.599
0.67
0.27534
2.78
0.0416
1.50
262.5
3.9
247.0
6.1
TIS-1/14
525.1
1223.6
40.1
2.330
1.91
0.29241
4.65
0.0423
1.69
267.3
4.4
260.5
10.7
TIS-1/15
638.3
516.9
36.4
0.810
0.14
0.30881
1.70
0.0437
1.51
275.5
4.1
273.3
4.1
TIS-1/16
482.7
282.3
24.6
0.585
0.41
0.28907
2.15
0.0413
1.50
260.7
3.8
257.8
4.9
TIS-1/17
341.2
165.8
17.3
0.486
0.32
0.30253
1.83
0.0422
1.50
266.2
3.9
268.4
4.3
TIS-1/18
376.0
204.7
18.6
0.544
0.42
0.27788
2.34
0.0407
1.70
257.1
4.3
249.0
5.2
TIS-1/19
750.9
496.8
41.1
0.662
0.35
0.30995
1.66
0.0434
1.50
273.7
4.0
274.1
4.0
Table 1: SIMS zircon U–Th–Pb data of the rhyolite sample TIS-1 (Tisovec-Rejkovo).
sample/spot
U
Th
Pb
Th/U
f
206
207
Pb/
235
U
±σ
206
Pb/
238
U
±σ
206
Pb/
238
U
±σ
207
Pb/
235
U
±σ
(ppm)
(ppm)
(ppm)
(%)
(%)
(%)
age (Ma)
(Ma)
age (Ma)
(Ma)
TEL-1/1
112.1
79.5
5.9
0.709
1.25
0.29439
2.38
0.0410
1.51
259.0
3.8
262.0
5.5
TEL-1/2
43.5
16.0
2.1
0.368
0.37
0.29479
4.75
0.0412
1.74
260.5
4.4
262.3
11.0
TEL-1/3
181.0
105.8
9.4
0.585
0.68
0.29764
2.08
0.0419
1.50
264.4
3.9
264.6
4.8
TEL-1/4
220.5
179.4
12.0
0.813
0.61
0.29205
1.99
0.0420
1.51
265.3
3.9
260.2
4.6
TEL-1/5
283.7
191.0
46.6
0.673
0.62
1.15836
2.18
0.1283
1.58
778.1
11.6
781.2
11.9
TEL-1/6
179.9
125.8
9.5
0.699
0.55
0.29307
2.09
0.0418
1.50
264.0
3.9
261.0
4.8
TEL-1/7
119.3
82.0
6.3
0.688
0.76
0.29592
2.43
0.0415
1.68
262.0
4.3
263.2
5.7
TEL-1/8
141.5
79.5
7.2
0.562
0.91
0.27857
4.42
0.0415
1.51
262.3
3.9
249.5
9.8
TEL-1/9
234.0
202.5
12.7
0.865
0.69
0.27604
3.36
0.0415
1.51
262.1
3.9
247.5
7.4
TEL-1/10
128.1
89.9
6.8
0.702
0.72
0.29547
2.27
0.0418
1.50
263.8
3.9
262.9
5.3
TEL-1/11
230.3
148.8
12.1
0.646
0.42
0.30028
2.06
0.0423
1.50
267.4
3.9
266.6
4.9
TEL-1/12
281.0
131.1
14.0
0.466
0.38
0.30170
1.89
0.0417
1.50
263.2
3.9
267.7
4.5
TEL-1/13
216.5
123.2
11.1
0.569
0.36
0.29609
1.98
0.0417
1.50
263.3
3.9
263.3
4.6
TEL-1/14
239.6
150.5
12.7
0.628
0.44
0.30755
1.95
0.0421
1.50
266.1
3.9
272.3
4.7
TEL-1/15
89.5
47.6
4.6
0.532
0.53
0.28974
2.56
0.0422
1.53
266.3
4.0
258.4
5.8
TEL-1/16
92.0
52.6
4.7
0.571
0.72
0.28760
2.53
0.0415
1.50
262.0
3.9
256.7
5.8
TEL-1/18
198.5
107.4
10.2
0.541
0.24
0.29556
2.55
0.0419
1.50
264.7
3.9
262.9
5.9
TEL-1/19
223.0
144.0
11.5
0.646
0.41
0.29354
1.98
0.0414
1.50
261.4
3.9
261.3
4.6
TEL-1/20
112.0
77.2
5.9
0.689
0.73
0.29815
2.71
0.0417
1.54
263.5
4.0
265.0
6.3
Table 2: SIMS zircon U-Th-Pb data of the rhyolite sample TEL-1 (Telgárt–Gregová Hill).
194
ONDREJKA , LI , VOJTKO, PUTIŠ, UHER and SOBOCKÝ
GEOLOGICA CARPATHICA
, 2018, 69, 2, 187–198
and volcano-sedimentary rocks in the Permian successions of
the Gemeric unit and in the Meliatic Bôrka nappe in the Inner
Western Carpathians (Vozárová et al. 2009, 2012; Kohút et
al. 2013).
The specific geochemistry of the dated rhyolites also reveals
their origin in an extensional regime of the crust. Despite their
unusual K-enrichment, the geochemistry indicates affinity to
alkali volcanic suites rich in Si, Rb, Zr, Y and REE and
depleted in Mg, Ca, Na, P, Sr, Ba and V; closely comparable to
hot and dry anorogenic A-type granitic rocks (Whalen et al.
1987; Eby 1990; Frost & Frost 1997; Frost et al. 2001). Zircon
typology (Pupin 1980) and saturation thermometry (Watson &
Harrison 1983) also support the solidification from high tem-
perature and alkali magma (Uher et al. 2002 b).
Finally, it should be noted that
the portrayed rhyolites occur only
in the Muráň nappe and its equi-
valent Vernár and Drienok nappe
fragments thrust far to the north
over the Veporic thick-skinned
thrust sheet. However, the typical
Silicic Unit, overlying the Meliata
and Gemeric units, does not con-
tain rhyolite volcanics. For that
reason, the aforementioned nappes
with the signatures of the rhyolite
volcanism do not necessarily
belong to the Silicic Unit (cf.
Havrila 1997; Vojtko 2000; Mello
et al. 2000 b; Vojtko et al. 2015),
but potentially to a specific group
of higher nappes in the Inner Wes-
tern Carpathians derived from the
northern margin of the Neotethys
Meliata(-Hallstatt) Basin, with
lacking the HP Meliatic (Bôrka
Nappe) fragments in the footwall.
Table 3: SIMS zircon U-Th-Pb data of the rhyolite sample SD-2 (Veľká Stožka-Dudlavka).
sample/spot
U
Th
Pb
Th/U
f
206
207
Pb/
235
U
±σ
206
Pb/
238
U
±σ
206
Pb/
238
U
±σ
207
Pb/
235
U
±σ
(ppm)
(ppm)
(ppm)
(%)
(%)
(%)
age (Ma)
(Ma)
age (Ma)
(Ma)
SD-2/1
531.3
358.4
28.7
0.674
0.37
0.30681
1.81
0.0427
1.50
269.8
4.0
271.7
4.3
SD-2/2
333.1
621.6
18.3
1.866
1.66
0.26071
3.85
0.0378
1.51
239.0
3.5
235.2
8.1
SD-2/3
732.5
626.0
40.8
0.855
0.10
0.30108
1.72
0.0425
1.50
268.1
3.9
267.2
4.1
SD-2/4
290.6
208.2
16.0
0.716
0.25
0.30484
1.88
0.0428
1.50
270.3
4.0
270.2
4.5
SD-2/5
530.7
246.8
27.1
0.465
0.19
0.30571
1.74
0.0427
1.50
269.3
4.0
270.8
4.1
SD-2/6
393.4
118.8
19.8
0.302
0.08
0.31167
1.85
0.0438
1.50
276.5
4.1
275.5
4.5
SD-2/7
620.2
483.5
34.4
0.780
0.04
0.30307
1.69
0.0428
1.50
269.9
4.0
268.8
4.0
SD-2/8
391.8
187.6
20.9
0.479
0.10
0.31258
1.81
0.0444
1.54
280.2
4.2
276.2
4.4
SD-2/9
575.4
445.6
32.0
0.774
0.33
0.30986
1.77
0.0430
1.50
271.6
4.0
274.1
4.3
SD-2/10
524.9
256.6
26.8
0.489
0.19
0.30338
1.72
0.0425
1.50
268.5
4.0
269.0
4.1
SD-2/11
397.1
275.6
21.8
0.694
0.32
0.31154
1.81
0.0434
1.53
273.8
4.1
275.4
4.4
SD-2/12
748.3
706.3
41.7
0.944
0.55
0.29073
2.11
0.0420
1.50
264.9
3.9
259.1
4.8
SD-2/13
412.6
330.9
21.5
0.802
0.48
0.29523
2.35
0.0412
1.50
260.3
3.8
262.7
5.4
SD-2/14
516.6
349.9
27.8
0.677
0.37
0.30374
1.73
0.0425
1.50
268.4
3.9
269.3
4.1
SD-2/15
526.3
372.2
28.5
0.707
0.23
0.30162
1.91
0.0425
1.50
268.1
3.9
267.7
4.5
SD-2/16
565.0
389.9
30.9
0.690
0.23
0.30448
2.20
0.0431
1.50
272.0
4.0
269.9
5.2
SD-2/17
605.0
295.4
31.0
0.488
0.21
0.30560
1.73
0.0425
1.52
268.3
4.0
270.8
4.1
SD-2/18
257.2
172.6
13.9
0.671
0.86
0.30208
2.11
0.0427
1.50
269.7
4.0
268.0
5.0
SD-2/19
474.4
412.6
26.6
0.870
1.00
0.29340
2.08
0.0425
1.50
268.5
4.0
261.2
4.8
SD-2/20
333.3
128.1
16.6
0.384
0.31
0.29651
1.88
0.0424
1.51
267.9
4.0
263.7
4.4
260
280
0.038
0.040
0.042
0.044
0.046
0.24
0.26
0.28
0.30
0.32
0.34
206
Pb/
238
U
207
Pb/
235
U
Concordia Age = 266.6 ±2.4 Ma
(95% confidence, decay-const. errs included)
MSWD (of concordance) = 1.3,
Probability (of concordance) = 0.25
Fig. 5. SIMS zircon U–Pb concordia age plots for rhyolite sample TIS-1 (Tisovec-Rejkovo).
195
PERMIAN A-TYPE RHYOLITES OF THE MURÁŇ NAPPE, INNER WESTERN CARPATHIANS
GEOLOGICA CARPATHICA
, 2018, 69, 2, 187–198
The presence of Permian granitic and rhyolitic magmatism
in the Western Carpathian area indicates their similarity to the
West-Mediterranean magmatic province (Bonin 1990, 1993,
1998; Deroin & Bonin 2003) and possible palaeogeographic
position in the “southern” branch of Variscan and post-
Variscan Europe, together with recent Alpine and Dinaride
terrains. Evidence of metamorphism related to Permo–Triassic
lithosphere thinning is documen ted in the neighbouring Eastern
Alps (Thöni 1999; Schuster et al. 2001). Correspondingly,
Permian acid volcanites and associated ignimbrites are also
widespread in the Southern Alps and are correlated with the
Bolzano Volcanic Complex (Cortesogno et al. 1998; Klötzli et
al. 2003; McCann et al. 2008;
Cassinis et al. 2012). Moreover,
Permian (Cisuralian) volcanism
was also documented in the
Mecsek and Apuseni Mts. (Balogh
& Kovách 1973; Bleahu et al.
1981; Stan 1984; Seghedi et al.
2001; Nicolae et al. 2014) and
in the Eastern and Southern
Carpathians and Carpatho–Balka-
nides to Balkanides (Stan 1987;
Kräutner 1997; Krstić & Karamata
1992; Cortesogno et al. 2004).
The Permian volcanic activity in
all these areas suggests an exten-
sional tectonic regime traditio-
nally interpreted as being related
to Pangea supercontinent break-up.
The Muráň Nappe A-type rhyo-
lites and their plutonic equivalents
represented by A-type granites
(Hrončok, Turčok, Upohlav, and
Velence), and most likely also the
rare metal S-type granites of the
Gemeric Unit, originated under
a transtensional or extensional
regime (Petrík et al. 1995; Uher
& Broska 1996). These plutonic-
volcanic processes are related to
post-orogenic (post-Variscan) large-
scale crustal extension and contem-
poraneous overlap with the initial
continental rifting stage of the new
Alpine cycle (Putiš et al. 2000,
2016). These tectono–magmatic
events are generally considered
to have been related to the ope-
ning of the Neotethys Ocean
(Ziegler & Stampfli 2001; Vai 2003;
Muttoni et al. 2009; Cassinis et al.
2012) and the Pangea break-up
(Isozaki 2009).
The change in geochemical
trend from collision-related calc-
alkaline to post-orogenic/anoro-
genic intracontinental alkaline
magmatic suites is clearly docu-
mented across Variscan Europe
(Bonin 1990, 1993, 1998) and
also in other regions worldwide
250
260
270
280
0.039
0.041
0.043
0.045
0.24
0.26
0.28
0.30
0.32
0.34
206
Pb/
238
U
207
Pb/
235
U
Concordia Age = 263.3 ±1.9 Ma
(2s, decay-const. errs included)
MSWD (of concordance) = 0.16,
Probability (of concordance) = 0.69
260
280
0.038
0.040
0.042
0.044
0.046
0.26
0.28
0.30
0.32
0.34
206
Pb/
238
U
207
Pb/
235
U
Concordia Age = 269.5 ±1.8 Ma
(2s, decay-const. errs included)
MSWD (of concordance) = 0.19,
Probability (of concordance) = 0.66
Fig. 6. SIMS zircon U-Pb concordia age plots for rhyolite sample TEL-1 (Telgárt).
Fig. 7. SIMS zircon U-Pb concordia age plots for rhyolite sample SD-2 (Veľká Stožka-Dudlavka).
196
ONDREJKA , LI , VOJTKO, PUTIŠ, UHER and SOBOCKÝ
GEOLOGICA CARPATHICA
, 2018, 69, 2, 187–198
(e.g., Nikishin et al. 2002). New models of Permian magma-
tism and metamorphism suggest mantle plums triggering both
the mantle and continental crust melting in the extensionally
thinned underplated lithosphere (e.g., Nikishin et al. 2002;
Sinigoi et al. 2011, 2016; Klötzli et al. 2014; Kunz et al. 2018).
Acknowledgments: We thank Xiaoxiao Ling, Jiao Li and
Hongxia Ma for assistance in SIMS U–Pb zircon analysis and
R.J. Marshall for polishing the English language. This work
was supported by the Slovak Research and Development
Agency (contracts APVV-14-0278, APVV-0315-12, APVV-
15-0050), the China Ministry of Science and Technology
(2016YFE0203000) and the VEGA Agency (Nos. 1/0257/13,
1/0279/15 and 1/0499/15). Finally, we thank Urs S. Klötzli,
Ľubomír Hraško and Igor Petrík (Handling editor) for their
constructive suggestions.
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