GEOLOGICA CARPATHICA
, DECEMBER 2019, 70, 6, 512–530
doi: 10.2478/geoca-2019-0030
www.geologicacarpathica.com
Exhumation history of the Variscan suture:
Constrains on the detrital zircon geochronology
from Carboniferous–Permian sandstones
(Northern Gemericum; Western Carpathians)
ANNA VOZÁROVÁ
1,
, KATARÍNA ŠARINOVÁ
1
, DUŠAN LAURINC
2
, ELENA LEPEKHINA
3
,
JOZEF VOZÁR
4
, NICKOLAY RODIONOV
3
and PAVEL LVOV
3
1
Comenius University in Bratislava, Faculty of Natural Sciences, Department of Mineralogy and Petrology, Mlynská dolina, Ilkovičova 6,
842 15 Bratislava, Slovakia;
anna.vozarova@uniba.sk, katarina.sarinova@uniba.sk
2
State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 04, Bratislva 11, Slovakia; dusan.laurinc@geology.sk
3
Centre of Isotopic Research, A.P. Karpinsky Russian Geological Research Institute (FGBU «VSEGEI»), Sredny prospekt 74,
199 106 St.-Petersburg, Russia; Nickolay_Rodionov@vsegei.ru, Elena_Lepekhina@vsegei.ru, Pavel_Lvov@vsegei.ru
4
Earth Science Institute of the Slovak Academy of Sciences, Dúbravská cesta 9, P. O. BOX 106, 840 05 Bratislava, Slovakia; jozef.vozar@savba.sk
(Manuscript received June 19, 2019; accepted in revised form October 25, 2019)
Abstract: The Late Paleozoic sedimentary basins in the Northern Gemericum evolved gradually in time and space
within the collisional tectonic regime of the Western Carpathian Variscan orogenic belt. The detrital zircon age spectra,
obtained from the Mississippian, Pennsylvanian and Permian metasediments, have distinctive age distribution patterns
that reflect the tectonic setting of the host sediments. An expressive unimodal zircon distribution, with an age peak at
352 Ma, is shown by the basal Mississippian metasediments. These represent a relic of the convergent trench-slope
sedimentary basin fill. In comparison, the Pennsylvanian detrital zircon populations display distinct multimodal distri-
butions, with the main age peaks at 351, 450, 565 Ma and smaller peaks at ~2.0 and ~2.7 Ga. This is consistent with
derivation of clastic detritus from the collisional suture into the foreland basin. Similarly, the Permian sedimentary
formations exhibit the multimodal distribution of zircon ages, with main peaks at 300, 355 and 475 Ma. The main difference,
in comparison with the Pennsylvanian detrital zircon assemblages, is the sporadic occurrence of the Kasimovian–
Asselian (306–294 Ma), as well as the Artinskian–Kungurian (280–276 Ma) igneous zircons. The youngest magmatic
zircon ages nearly correspond to the syn-sedimentary volcanic activity with the depositional age of the Permian host
sediments and clearly indicate the extensional, rift-related setting.
Keywords: detrital zircon, U–Pb SHRIMP dating, provenance, tectonic setting.
Introduction
The kinematic evolution of the Western Carpathian orogenic
system was created during both Variscan and Alpine orogeny.
Fragments of newly formed Variscan crust were incorporated
into the Alpine Western Carpathian units, which documents
the repeating subduction/collision and transform fault pro-
cesses. The Variscan crust was gradually amalgamated due to
crustal thickening during Devonian/Mississippian collision
events. The Tournaisian/Visean deep-water turbidite trough in
the Northern Gemericum, originated in a convergent embay-
ment and was continued as a Pennsylvanian peripheral basin.
The Upper Pennsylvanian/Permian post-collisional evolution
of the Western Carpathian realm continued by development of
transtension/transpression and rift-related continental sedimen-
tary basins.
Fragments of the Late Paleozoic sedimentary basin fillings
are only preserved inside of the internal structural zone of
the Alpine Western Carpathian orogeny. They became a part
of the principal crustal-scale Alpine units of the Central and
Inner Western Carpathians. These are arranged in an order
from N to S and from bottom to top in the Tatricum, Vepori-
cum, Northern and Southern Gemericum and several cover
nappe systems (Fatricum, Hronicum, Bôrka Nappe as a part of
Meliaticum, Turnaicum and Silicicum) (Biely et al. 1996a, b;
Plašienka et al. 1997; Rakús et al. 1998; Plašienka 2018 and
references therein).
Relics of the Carboniferous–Permian sedimentary sequences
are present in the relatively wide range of sedimentary envi-
ronments, evolving from deep-water through shallow-marine
to paralic and continental. Within the framework of the whole
Western Carpathian belt, the remnants of sedimentary rocks
from this wide succession of sedimentary environments, and
moreover in direct temporal sequence, are preserved only in
the Northern Gemeric Unit (NGU; Fig. 1),. Petrofacial ana-
lysis of the Carboniferous–Permian sediments (Vozárová
1998 a, b), supplemented by the detrital zircon geochronology,
directly reflects the process of tectono–thermal evolution and
exhumation of the Variscan collision suture in the Western
Carpathians. The U–Pb age dating of detrital zircons from this
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area was completed for the first time by Vozárová et al. (2013).
From the NGU Carboniferous–Permian sediments, 172 zircon
ages were obtained, with a relatively wide age variance, ran-
ging from 260 to 2700 Ma. Their mutual proportions were
gradually changing, depending on the lithostratigraphy and
time-scale, from the oldest to the youngest sediments. To this
data set 126 new zircon data have been added with the inten-
tion of obtaining more detail background for interpretation.
Geological setting of the NGU
Carboniferous–Permian sedimentary sequences
The NGU zone contains relics of the Variscan collision
suture, characterized by thrust wedges of the two pre-Carbo-
niferous terranes, the medium/high-grade gneiss–amphibolite
Klátov Complex and the low-grade Rakovec Complex, and
relics of the Mississippian syn-orogenic deep-water turbidite
sequence. Pennsylvanian shallow-marine to paralic and Per-
mian continental sedimentary basins postpone the main colli-
sional events (e.g., Bajaník et al. 1983; Spišiak et al. 1985;
Vozárová & Vozár 1988; Hovorka et al. 1988; Németh
2002; Németh et al. 2004; Ivan 2009; Radvanec et al. 2017).
Defor mational and metamorphic events recorded in both pre-
Carboniferous terranes occurred in the Late Devonian–
Mississippian, which is documented by their reworked rock
fragments within the overstepping Pennsylvanian conglome-
rates (Krist 1954; Vozárová 1973, 2001) and by several geo-
chronological data (Vozárová et al. 2005, 2013; Putiš et al.
2008, 2009a). Those terranes experienced Alpine reworking
(Dallmeyer et al. 1996, 2005; Lexa et al. 2003; Vozárová et al.
2005, 2014; Putiš et al. 2009b).
Mississippian: The Mississippian formations have been pre-
served as tectonic relics at the W-SW and E-SE boundary of
the NGU. These suffered a significant shortening as a result of
Alpine thrusting of the NGU on the underlying Southern
Veporicum in the footwall along the Lubeník–Margecany Line
(LML; Andrusov 1959) (Fig. 1). Equally, the tectonic contact
of the NGU with the Southern Gemericum is represented by
the Hrádok–Železník Line (HZL) in the hanging wall (defined
by Abonyi 1971), which continues into a system of thrust
faults to the east (Fig. 1). The Mississippian turbidite wedges,
supposedly derived from the Variscan suture, were interpreted
as the fill of an intrasuture remnant ocean basin (Vozárová &
Vozár 1988) or foredeep basin (Neubauer & Vozárová 1990;
Ebner et al. 2008). In spite of orogenic/metamorphic reduction
the present thickness of the Mississippian formations is esti-
mated >1000 m (Vozárová 1996). A completely different
opinion on the genesis of the Mississippian rock sequence
was given by Novotná et al. (2015). The authors interpreted
Fig. 1. Geological sketch of the Northern Gemericum (modified according to Biely et al. 1996 and Bajaník et al. 1984a), showing localities of
the studied detrital zircon samples. Abbreviations: LML — Lubenik–Margecany Line; HZL — Hrádok–Železník Line.
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the basal part of the Ochtiná Group (the Hrádok Fm. according
to the lithostratigraphic classification by Vozárová 1996,
Fig. 2) as a tectonic melange formed during the Cretaceous
collision at the boundary of two major crustal nappes, the
Gemericum and Veporicum. It is, however, necessary to empha-
size that the Mississippian succession represents a sedi mentary
formation with typical features of deep-water turbidite sedi-
mentation, but certainly strongly tectonically reworked during
the Cretaceous orogenic processes.
The whole Mississippian sequence was deformed in the P–T
conditions of greenschist facies. Fine-grained muscovite from
the Hrádok Formation reflects the complex Alpine overprint
Fig. 2. Schematic lithostratigraphic columns of the Carboniferous–Permian sedimentary formations in the Northern Gemericum (modified after
Bajaník et al. 1981; Vozárová 1996 and Vozárová et al. 2015) with sample locations. a — W and SW part; b — N part; c — E and SE part.
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(
40
Ar/
39
Ar — 87 Ma at the rim to 142 Ma in the core, Vozárová
et al. 2005;
40
Ar/
39
Ar — 84 Ma, Putiš et al. 2009b). The Missis-
sippian volcano-sedimentary sequence, defined by Vozárová
(1996) as the Ochtiná Group (Fig. 2), is represented by the
deep-water turbidite sediments in its lower part (the Hrádok
and Črmeľ formations) and shallow-water, shaly-carbonate
sediments in its upper part (Lubeník Formation, inclusive
Bankov Beds).
The Hrádok Formation (Fm.) consists of a dark-grey and
black clastic turbidite sequence, metaparaconglomerates, meta-
sandstones, and metapelites, interlayered with metabasalts,
metamicrodolerites and basic metavolcaniclastics. Sporadic
lydites and siliceous metapelites were found only in thin layers
and lenses. Slabs of ultramafic rocks (oceanic crust fragments)
represented by antigorite serpentinites and tremolite-talc schists
and scarce amphibolites as well as actinolite green-schists
are integral part of this deep-water turbidite slope/rise
sequence. A monotonous complex of dark-grey and black
metapelites, overlying the relatively coarser-grained basal part
of the Hrádok Fm., yielded a microflora indicating the Upper
Turnaisian–Visean age (Bajaník & Planderová 1985).
The Mississippian sequence of the Črmeľ Fm. (Fig. 2c)
represents a distal turbidite complex consisting of alternating
metapelites, fine-grained metasandstones, basic to interme-
diate metavolcanics and its metavolcaniclastics, subsidiary
carbonates and lydites (Bajaník et al. 1984a; Grecula 1998).
Small amounts of acid volcanoclastic detritus are unevenly
dispersed in its basal part. The Tournaisian–Visean age of
the Črmeľ Fm. was indicated by microflora assemblages by
Snopková in Bajaník et al. (1984b).
The overall upward-shallowing Mississippian sequence is
interpreted as a reflection of progressive basin filling. The youn-
gest Mississippian sedimentary rocks (Lubeník Fm.; Vozárová
1996; Fig. 2) are represented by the Upper Visean–Serpu-
khovian black shales and bioclastic carbonates, well documen-
ted by fauna, mainly in the western part of their occurrences
(Bouček & Přibyl 1960; Kozur et al. 1976; Zágoršek & Macko
1994; Mamet & Mišík 2003).
Pennsylvanian: The Pennsylvanian transgressive sequence
rests unconformably on the two NGU pre-Carboniferous com-
plexes (Klátov and Rakovec) and, also, on the Mississippian
succession in the E-SE realm of NGU (Fig. 2) and fix up
the Variscan thrust/nappe structure. The Upper Bashkirian–
Moscovian sequence started after a break of sedimentation,
with boulder to coarse-grained delta-fan conglomerates
(the Rudňany Fm., Fig. 2). They contain a detritus derived
from both pre-Carboniferous complexes (Klátov and Rako-
vec), as well as, from the Mississippian sedimentary rocks
(Krist 1954; Vozárová 1973; Vozárová & Vozár 1988).
How ever, sporadic “exotic rocks”, which do not occur on
the NGU surface today, were found. They include pebbles of
plagio granites, granitoides, orthogneisses and metaquartzites
(Vozárová 1973, 2001). Black shales and mica-rich grey sand-
stone intercalations are normal members of the fining upward
Rudňany Fm. They contain Pennsylvanian macroflora remains
which were determined by Němejc (1947). The 370—380 Ma
40
Ar/
39
Ar cooling age data of white mica from metasandstones
and gneiss pebble indicate a first step of the Variscan colli-
sional suturing in the NGU zone (Vozárová et al. 2005). After
initial rapid sedimentation the littoral to shallow-neritic lime-
stones were associated with grey and black shales. This silici-
clastic–carbonate lithofacies correspond to the basal part of
the Zlatník Fm., which the Moscovian age is indicated by rich
trilobite (Rakusz 1932; Bouček & Přibyl 1960) and conodont
fauna (Kozur & Mock 1977).
The upper part of the Zlatník Fm. comprises fine-grained
clastic metasediments associated with basalts and their volca-
niclastics. Poor microfloral assemblages proved the Pennsyl-
vanian age, but not an accurate division. This succession was
formerly defined as the Zlatník Fm. (ZF) by Bajaník et al.
(1981). However, Ivan (1997) and Ivan & Méres (2012) sepa-
rated this complex of basic metavolcanics and metavolcani-
clastics, associated with small amounts of fine-grained
metasediments from the ZF. The authors defined this new
lithostratigraphic unit as the Zlatník Group. This strongly con-
tradicts the priority rule of the stratigraphic code (Michalík et
al. 2007). If we assume that this set of basic volcanic lies in
the tectonic position on the basal sediments of the ZF strata,
then it should be included in the pre-Carboni ferous NGU
basement, most likely in the Rakovec Complex. This would
also be indicated by the detected zircon ages from the ZF basic
metavolcaniclastic, aged from 478 to 521 Ma (only four zircon
grains, Vozárová unpublished data), as well as 388–382 Ma
magmatic age from metabasalts (Putiš et al. 2009a). However,
such a low number of zircon data does not entitle us to con-
sider such an interpretation.
Termination of the Pennsylvanian peripheral basin is ref-
lected by the paralic sequence of the Hámor Fm. (Fig. 2). It is
characterized by distinct cyclical coarsening-upward shaly–
sandy–conglomeratic sediments, an absence of synsedimen-
tary volcanism and a local occurrence of ribbed coal seam.
Poor microflora assemblages proved uppermost Moscovian
age (Planderová & Vozárová 1980).
Permian: Continental Permian red-beds unconformably
overlapped slightly deformed relics of the Moscovian periph-
eral basin filling, as well as two pre-Carboniferous NGU crys-
talline complexes and the Mississippian sequences (Fig. 2).
Prevalent clastic sediments derived from the collision belt are
associated with andesite/basalt–rhyolite volcanism (Rojkovič
& Vozár 1972; Václav & Vozárová 1978; Bajaník et al. 1981,
1983; Novotný & Miháľ 1987; Rojkovič & Miháľ 1991 and
references therein). The basal part (Knola Fm.) contains
mostly poorly sorted polymictic conglomerates and breccias
of extremely variable thickness, with pebble material reflec-
ting the composition of the direct underlier (fossil mudflows
relieved by alluvial, mainly stream channels, Vozárová 1996,
1998b). The polyphase volcanic activity manifested large
sedi mentary cycles. Sediments are characterized by a low
degree of maturity and mixture of volcanic and non-volcanic
detritus. The most striking features are the fining-upward allu-
vial cycles, with channel lag, point-bar and floodplain facies,
alternating with playa at the topmost part of the large cycles.
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The existing monazite and U–Pb SHRIMP zircon ages yield
Cisuralian ages (Kungurian) for both, the acid and basic volca-
nic members (278 Ma — monazite, Rojkovič & Konečný
2005; 272–275 Ma — U–Pb zircon ages, Vozárová et al. 2012).
The last volcanic phase was linked with extension at the Per-
mian–Triassic boundary, connected with the beginning of
the Alpine orogenic cycle (257.2 ± 3.0 and 255.6 ± 3.7 Ma
Re–Os molybdenite ages, Kohút et al. 2013; 251 ± 4 Ma U–Pb
zircon ages, Vozárová et al. 2015).
The NGU Permian–Triassic volcanic event seems to be
approximately coeval with the sedimentation of the Novoveská
Huta Fm. evaporite member that is correlated with the Zech-
stein (Continental Stage) based on S and O isotopes (Kantor
et al. in Vozárová 1997). The polymictic conglomerates
(the Strážany Beds; Miháľ in Rojkovič & Miháľ 1991) that
underlie this evaporate lithofacies, contain fragments of volca-
nics, which were redeposited from the Cisuralian volcanic
suite. On the account of that, the stratigraphic gap from the
mid-Guadalupian to the Lopingian, is supposed to be trust-
worthy (Vozárová et al. 2015) (Fig. 2c).
Analytical methods
The rock-forming minerals were studied by an electron
microprobe (CAMECA SX-100, in the laboratory of the Geo-
logical Survey of Slovak Republic, Bratislava). Zircons have
been extracted from the rocks by standard grinding, heavy
liquid and magnetic separation analytical techniques. The inter-
nal structure of individual zircon crystals was examined
with cathodoluminescence (CL) imaging by SEM (CamScan
M2500 Oxford Instruments). In situ U–Pb analyses were per-
formed using a Sensitive High-Resolution Ion Microprobe
(SHRIMP-II) at the Centre of Isotopic Research (CIR) in
A.P. Karpinsky Russian Geological Institute (VSEGEI), by
applying a secondary electron multiplier in peak-jumping
mode, based on the procedure described by Williams (1998).
Primary beam size allowed for the analysis an area of ca.
25×20 µm. CL, BSE and optical (transmitted light) imaging
was applied to reveal the internal and surface features that
were used to choose the position of analytical spots on the
mostly homogeneous inclusion-free parts of individual zircon
grains. The 80 µm wide ion source slit, in combination with
a 100 µm multiplier slit, allowed for the mass-resolution
M/∆ M ≥ 5000 (1% valley); hence, all the possible isobaric
interferences were resolved. The following ion species were
measured in the sequence:
196
(Zr
2
O) –
204
Pb – background
(ca.
204.5
AMU) –
206
Pb –
207
Pb –
208
Pb –
238
U –
248
ThO –
254
UO. At least
4 mass-spectrums were acquired for each analysis. Zircon
Temora-1 (Black et al. 2003) was measured as the main refe-
rence material (RM): one analysis per every four analyses
of unknowns to obtain their U/Pb ratios. Zircon 91500
(Wiedenbeck et al. 1995) was used as a concentration RM.
The obtained results were processed by the SQUID v1.12
(Ludwig 2005) and ISOPLOT/Ex 3.75 (Ludwig 2012) soft-
ware, with decay constants recommended by Steiger & Jäger
(1977), including modern corrections, e.g. Hiess et.al (2012).
Common lead correction was done on the basis of the mea-
sured
204
Pb/
206
Pb ratio. The ages given in this text, if not addi-
tionally specified, are
207
Pb/
206
Pb for zircon older than 1.0 Ga,
and
206
Pb/
238
U for those younger than 1.0 Ga. The degree of
discordance was calculated according to the following for-
mula: % D =100 * (Age
207/206
/Age
206/238
−1). The uncertainties
are quoted at standard deviation level (1s, i.e. 68.3 % confi-
dence) for individual points and at 2 s level in the Concordia
diagram, for the Concordia ages or any previously published
ages discussed in the text. Age distributions of detrital zircons
are displayed as Kernel Density Estimates (Vermeesch 2012).
Only analyses that produced concordant ages within 10 %
(−10 < % D < +10) were used. The time-scale calibration of
the International Chronostratigraphic Chart (2018-8) was used
to compare geochronological data from detrital zircons with
fossil-bearing sedimentary units and tectono–thermal events.
Results
Sample characteristics
Seven samples have been processed for zircon dating from
the Carboniferous–Permian sandstones of the NGU succes-
sion (Figs. 1, 2). From one previously dated sample an addi-
tional zircon dating was made (LA-66; Vozárová et al. 2013).
Hrádok Fm.: The sample GZ-28 was collected from
the upper part of the Hrádok Fm., SE from the Sušanský vrch
elevation, along a forest road cut, 421 m above sea level (GPS
coordinates: 48°35.504’N, 20°03.076’E). This metasandstone
displays a strong foliation, with indication of crenulation
cleavage in places. Primary mineral composition was consi-
derably changed due to a strong Alpine deformation and
recrystallization. Quartz and detrital micas are the most fre-
quently preserved detrital grains. Primary clayey matrix and
feldspar clasts were recrystallized and became a fine-grained
aggregate of “pseudomatrix” (ca. 40 % of the whole rock).
This consists of quartz+muscovite±paragonite and graphite.
Rudňany Fm.: Two cobbles from the basal part of the Rud-
ňany Fm. were gathered for zircon dating. The sample GZ-36A
was collected from the forest slope cliff east of the Košická
Belá Village, 478 m above sea level (GPS coordinates:
48°48.443’N, 21°07.083’E). This is represented by the meta-
quartzite with non-uniform granoblastic texture and relics of
primary roundness on the surface of selected quartz grains.
Besides quartz grains (ca. 98 %) scarce fragments of acid
felsites and quartzose phyllites were recognized. Zircon, rutile
and tourmaline are common heavy minerals.
The cobble GZ-55 was taken from the forest cliff SE of
the Poráč Village, 650 m above sea level (GPS coordinates:
48°52.220’N, 20°42.531’E). It represents biotite–plagioclase
orthogneiss with a lepidogranoblastic texture that is characte-
rized by alternating light and dark bands differing in mineral
composition. The light bands contain mainly quartz and pla-
gioclase and only sporadic orthoclase. Plagioclases express
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an oligoclase composition range (Or =1 %, Ab =75 %, An = 24 %;
average from five analysis) (Supplement, Table S1). K-feldspar
is perthitic with microcline twinning in places. The darker
bands consist of biotite associated with small amounts of
garnet (Prp = 9 %, Sps = 5 %, Alm = 71 %, Grs =15 %; average
from three analyses). The minerals are oriented parallel to
schistosity. This gneissic rock was affected by powerful
secondary alteration, manifested by a sericitization of feld-
spars and a total chloritization of biotite and partially of gar-
net. Accessory apatite and zircon are present.
The sample GZ-35 represents the composition of sandstones
from the upper part of the Rudňany Fm. It was collected along
the small gorge at the E edge of the Košická Belá Village,
413 m above sea level (GPS coordinates: 48°48.317’N,
21°06.913’E). This coarse-grained sandstone is strongly folia-
ted, with individual greater clasts deformed along the foliation
planes. Quartz, detrital micas and lithic fragments of different
phyllites, mica schists and volcanics are the prevalent primary
association. Feldspars are present sporadically. Recrystallized
“pseudomatrix” is characterized by preferred orientation of
quartz–sericite aggregates, which most probably also involved
a part of the lithic fragment detritus.
Hámor Fm.: Two samples have been collected from the
Hámor Fm. The sample GZ-27 comes from western edge of
the Poproč Village, 555 m above sea level (GPS coordinates:
48°35.082’N, 20°01.950’E). As a consequence of a strong
Alpine deformation in the shear-zone along the LML (Fig. 1),
the metasandstone is strongly recrystallized and foliated.
The dominant part of the mineral composition is formed by
undulatory quartz grains, which have undergone a dynamic
recrystallization. Other immature detrital grains (supposed
feldspars or volcanic and lithic fragments) are completely
recrystallized into strongly preferred, fine-grained quartz +
sericite ± graphite aggregates. Detrital mica is distinguishable.
The sample 29-LA was collected along a regional road cut
1 km SW from the Margecany Village, 343 m above sea level
(GPS coordinates: 48°53.208’N, 21°00.339’E). Prevalent quartz
grains (73 %), associated with plagioclase (7 %), K-feldspar
(4 %), detrital mica (4 %) and lithic fragments (12 %) are
characteristic for the mineral composition of this quarzolithic
metasandstone. Various types of phyllites, fine-grained sand-
stone, lydite, acid volcanics and sporadically crystalline
schists have been identified among the lithic fragments.
The studied metasandstone is characterized by a massive,
partly foliated blastopsammitic texture. Dominant are the clas-
tic grains displaying a variable degree of pressure solution and
a fine-grained recrystallized matrix (on average 20 %), con-
sisting of quartz+sericite±chlorite, with preferred orientation.
Petrova Hora Fm.: The sample 74-LA was taken from
the eastern occurrences of the Petrova Hora Fm., 1.2 km W
from the Jaklovce Village, 361 m above sea level (GPS coor-
dinates: 48°52.131’N, 20°58.670’E). This sandstone displays
red-violet colour and immature mineral and textural composi-
tion, typical for “red-beds” facies. Among detrital grains the
quartz (55 %), plagioclase (8 %), K-feldspar (4 %), volcanic
and lithic fragments (16 %) and detrital micas (17 %) were
recognized. Relatively rich matrix (27 %) contains quartz,
sericite and abundant hematite pigment.
Novoveská Huta Fm.: No new sample was collected from
the Novoveská Huta Fm. The original sample LA-66, pub-
lished in the article Vozárová et al. (2013) has been supple-
mented by new 10 measurements that were once again
recalculated together with the older age data.
Zircon dating
Mississippian population
The detrital zircon age data were acquired from the sample
GZ-28, which was collected from the upper part of the Hrádok
Formation (Fig. 2). Comparison with the previously published
sample LA-81 (Vozárová et al. 2013), which was located in the
basal part of the Hrádok Formation, established the occurrence
of the Early Ordovician/Late Cambrian detrital zircon ages in
the range from 482 ± 5 to 509 ± 6 Ma (Fig. 3). All of them show
characteristic features of a magmatic origin, with the
232
Th/
238
U
ratio values between 0.29 and 0.39 and oscillation growth
zoning (Fig. 3c; Supplement, Table S2). One exception is rep-
resented by spot 12, which gave the 499 ± 4 Ma age (Fig. 4).
That was indicated by the narrow rim that mantled the oscilla-
tory zoned and corroded zircon core. The main characteristics
of spot 12 are low
232
Th/
238
U ratio value (0.09) and texture
indicating a local recrystallization.
The second group of detrital zircons is determined by the
Visean and Famennian ages. Two of them, 330 ± 2 and 367 ± 4 Ma
old, show the typical features of magmatic origin with fine
oscillation growth zoning and characteristic
232
Th/
238
U ratios
of 0.40 and 0.95, respectively. Two other zircon grains display
the age of 340 ± 2 and 368 ± 2 and low
232
Th/
238
U ratios of 0.02
and 0.04, respectively (Fig. 3c). Both zircons are preserved as
the homogeneous inherited cores, which were mantled by
the fine-oscillation growth zoned rims.
The last group of detrital zircon ages belongs to the Pre-
cambrian. One spot is 566 ± 6 Ma old (Ediacaran) and other
one 2045 ± 27 Ma old (Orosirian). Further three zircon grains
are ranging from 2694 ±13 to 2760 ± 8 Ma (Neoarchean).
Thus, the studied detrital zircon age distribution, shown by
the Probability Density Plot (PDP), identify the main peak at
the 340, 483 Ma and further smaller peaks at 568 and 2696 Ma
(Fig. 3b).
Pennsylvanian population
Rudňany Formation — basal part
The sample GZ-36A represents metaquartzite, indicating
the detrital origin of the all analysed zircon grains. From the
investigated detrital zircon set, Phanerozoic age was found in
only one zircon grain, which corresponds to the 537± 6 Ma
(lowermost Cambrian, Fortunian Stage) (Supplement, Table
S2). All others zircon data confirm the Precambrian with
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dominance of the Paleoproterozoic, ranging from 1888 ± 28 to
2136 ±13 Ma (7 grains) and the Neoarchean, ranging from
2514 ± 24 to 2770 ±11 Ma (7 grains). The last two zircon grains
gave the 2834 ± 20 and 2941± 22 Ma ages that document
Mesoarchean. Correspondingly, the remarkable age peaks on
the PDP are at 2028 and 2688 Ma age and smaller peaks at 537
and 576 Ma (Fig. 5). Evidently, the majority of the analysed
zircon grains show a typical feature of magmatic origin,
reflected by the
232
Th/
238
U ratio values within the range of
0.27–1.95 (Fig. 3c). This is also documented by the fine growth
oscillatory zonation. However, within the Paleozoic and
Archean zircons later recrystallization can be observed, which
has led to a gradual fading of original growth zoning. This
could be correlated with Pb loss, probably caused by a later
metamorphic recrystallization (Fig. 4). Among the studied
detrital zircon assemblage only one grain 2007±18 Ma is cha-
racterized by a very low
232
Th/
238
U ratio value (0.08) and
homogeneous internal texture, suggesting thus a metamorphic
origin (Fig. 3c; Supplement, Table S2).
The sample GZ-55, represented by the orthogneiss cobble,
displayed a further unique zircon population (Supplement,
Table S2). The Concordia diagram clearly shows the bimodal
distribution of the age data, corresponding to the Middle/
Upper Devonian and Cambrian, respectively (Fig. 5). Cam-
brian ages, ranging from 510 ±1.5 to 534 ± 2.5 Ma are domi-
nant. The
206
Pb/
238
U Concordia age, calculated from the three
concordant spots, gave 508.8 ± 4.3 Ma (Fig. 5). All of the ana-
lysed grains show the
323
Th/
238
U ratio values in the range of
0.20–0.39, indicating origin from acid magmatic rocks (Fig. 3c).
Relics of the fine oscillatory growth zoning is currently
observed, with some traces of recrystallization (enclaves of
convolute or patchy textures). A further two zircon grains pro-
duced younger ages, 504.4 ±1.6 Ma and 491.6 ± 3.8, and are
characterized by relatively lower
232
Th/
238
U ratio values, 0.08
and 0.10, respectively (Fig. 3c). This strongly indicates a late
magmatic or metamorphic recrystallization. It is necessary
to emphasize that all studied zircon grains are mantled by
the narrow light rims. Two of these rims, those that could be
Fig. 3. a — Selected sector of the Concordia from the sample GZ-28 (Hrádok Fm.) relevant to the most prominent cluster for age spectrum
from 750 to 350 Ma. b — Corresponding PDP of detrital zircon ages. c — Th/U ratios of detrital zircons from the NGU Carboniferous–Permian
metasediments vs. time scale.
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measured, were analysed and gave ages of 385.7±6.3 and
386.7±4.9 Ma that are almost equal within the error (Fig. 4).
The relatively low
232
Th/
238
U ratio values, 0.06 and 0.01,
respectively, indicate metamorphic recrystallization.
Rudňany Formation — upper part
This is represented by a detrital zircon population from
the sandstone samples GZ-35. The comparable detrital zircon
Fig. 4. Selected CL images of detrital zircons from the studied samples.
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groups are represented by the Tournaisian–Famennian ages,
ranging from 350.8 ± 5.2 to 363.9 ± 5.4 Ma. The
206
Pb/
238
U
Concordia age, calculated from the six concordant spots, gave
355.9 ± 4.3 Ma, which is well indicated by 356 Ma peak on
the PDP diagram (Fig. 6). The
232
Th/
238
U ratios of less than 1,
ranging between 0.30 and 0.84, as well as a growth zoning
indicate their derivation from an acid magmatic source
(Fig. 3c). The older Phanerozoic detrital zircons are 384.1± 5.5
and 497.1±7.7 aged, with
232
Th/
238
U ratio values of 0.35 and
0.27, respectively (Supplement, Table S2).
Next part of the GZ-35 detrital zircon set is formed by the
Precambrian population. From those two zircon grains yielded
Cryogenian, 671.7± 9.7 and 724.0 ±12 ages. The other grain
gave 781.0 ±13 Ma of Tonian age. Among these, only 671.7 Ma
zircon exhibits the
232
Th/
238
U ratio higher than 1 (1.95), what
reveals a basic magmatic source (Fig. 3c). A further five zircon
grains belong to the Mesoproterozoic (2028.0 ± 8 Ma), the Neo-
archean (2619.5 ± 8.3 and 2665.7± 9.7 Ma) and the Meso-
archean (2998.0 ±16 Ma). Based on the
232
Th/
238
U ratios,
the majority of these zircons demonstrate acid magmatic
sources. The only exception is the zircon grain 2028 Ma old
with 0.01
232
Th/
238
U ratio value, presumably indicating a meta-
morphic source (Supplement, Table S2).
Thus, the whole Rudňany Fm. zircon assemblage (samples
GZ-35 + GZ-36A + GZ-55) indicate the following four age peaks
on the PDP diagram: 356, 518, 2028 and 2688 Ma (Fig. 6.).
Hámor Formation
Two samples have been collected from the Hámor For-
mation; sample 29-LA from the eastern and sample GZ-27
from the western part of the NGU surface occurrences
(Figs. 1, 2).
Sample 29-LA: The youngest detrital zircon ages vary from
346.2 ± 5.8 to 383.0 ± 6.3 Ma (Fig. 7). Fine oscillation growth
zoning, as well as
232
Th/
238
U ratio values between 0.29 and 0.38
indicate derivation from an acid magmatic source (Fig. 3c; Sup-
plement, Table S2). The Middle Ordovician magmatic source
is documented by two grains, 464.7±7.5 and 453.0 ±7.6 Ma
old (
232
Th/
238
U ratios 0.36 and 055). Besides, the 475.7± 8 Ma
homogeneous metamorphic rim (
232
Th/
238
U ratio = 0.02),
the mantled old core 1269.0 ±7.1 was observed (Supplement,
Table S2). One solitary detrital zircon grain of 496.8 ± 8.1
(Furongian) was found. A frequent set of detrital zircons ran-
ges from 544.7± 8.8 Ma to 622.0 ±14 Ma. The Concordia age,
calculated from seven concordant data yielded 595.0 ±12 Ma,
which clearly represents the Ediacaran Period. Three further
zircon grains in the age of 724.0 ±13, 843.0 ±17 and
878.0 ±14 Ma correspond to the Tonian. The oldest zircons
detected are 2095.0 ±13 and 2195.0 ±10 Ma old. In general,
the distribution of detrital zircons ages is well presented on
the PDP with the main peaks at 468, 561 and 596 Ma and
small peak at ~2.1 Ga (Fig. 7).
The majority of the studied detrital zircons demonstrate
the
232
Th/
238
U ratio values less than 1, thus indicating acid
magmatic sources (Fig. 3c). Some Ediacaran zircons show
232
Th/
238
U ratio values in the range of 1.04–2.07, which could
specify an intermediate and/or mafic magmatic source
(Supplement, Table S2).
Sample GZ-27: Compared to the sample 29-LA, the age
spectrum of detrital zircons begins at the Moscovian, which is
denoted by the two grains of 308 ± 2 and 309 ± 2 Ma old (Fig. 7).
Both display by their oscillatory growth zoning and
232
Th/
238
U
ratio values of 0.85 and 0.28, respectively. One zircon grain
Fig. 5. a — Concordia plot of zircons from the Rudňany Fm.
metaquartzite cobble (GZ-36A). b — Corresponding PDP. c — Con-
cordia plot of zircons from the Rudňany Fm. gneiss cobble (GZ-55),
with indication of the Concordia age.
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revealed the 460 ± 5 Ma age (Middle Ordovician), characte-
rized by growth zoning and a relatively high
232
Th/
238
U ratio
value, equalling to 1.66 (Fig. 3c). The next group of zircons is
signified by three Cambrian grains, aged from 497± 4 to
522 ± 9 Ma. All display the growth zoned internal texture and
232
Th/
238
U ratio values in the range of 0.61–1.22, which indi-
cate derivation from an acid/intermediate magmatic source
(Fig. 3c; Supplement, Table S2). The whole age spectrum of
detrital zircon ages is clearly visible on the PDP, especially
the peaks at 309 and 502 Ma, and two sub-peaks at 578 and
2450 Ma (Fig. 7).
More than half the studied detrital zircon grains proved
Precambrian ages (Supplement, Table S1). From these, one
grain is identical with Ediacaran, of the 577± 6 Ma aged.
A further nine zircon grains are scattered from 2066 to
2936 Ma. Three of them express the Paleoproterozoic, ranging
from 2066 ± 38 to 2451±13 Ma and additional two Neoarchean
of 2552 ±15 and 2681±15 Ma. The oldest group of detrital zir-
cons belong to the Mesoarchean with ages of 2709 ±15,
2832 ± 26 and 2936 ±13 Ma (Supplement, Table S1).
Permian population
Petrova Hora Formation
The cluster of detrital zircon data from the sample 74-LA
yielded concordant ages, mainly between 298 and 493 Ma
(Fig. 8; Supplement, Table S2). The youngest detrital zircon gave
the age of 298.4 ± 5.7 and 303.4 ± 6.8 Ma, both almost within
the analytical errors. They display a fine-oscillation growth
zoning and 0.34 and 0.30
232
Th/
238
U ratio values, compatible
with an acid magmatic source (Fig. 3c). The 300.8 ± 8.1 Ma
Concordia age has been provided from these two data. How-
ever, among the studied detrital zircon set, Late Devonian–
Mississippian ages, ranging from 346.4 ± 6.6 to 379.4 ±7.2 Ma
are prevalent, with
232
Th/
238
U ratios from 0.14 to 0.69.
The Concordia age, calculated from four concordant spots,
gave 353.4 ± 6.5 Ma (Fig. 8). Rare Silurian ages were deter-
mined for two grains. The first grain documents a magmatic
event at 434 ± 8 Ma with
232
Th/
238
U ratio value of 0.40.
The second grain corresponds to the 433 ± 9 Ma of the Middle
Fig. 6. Concordia plot of detrital zircons from the upper part of the Rudňany Fm. (GZ-35). a — all detrital zircon ages. b — Selected sector for
age spectrum from 340 to 380 Ma, showing the Concordia age of prominent detrital zircon population. c — Corresponding PDP. d — PDP
diagram for the all dated zircons from the Rudňany Fm. (GZ-35, GZ-36A, GZ-55).
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Silurian metamorphic event and has a characteristic low
232
Th/
238
U ratio value (= 0.01). Three detrital zircon grains
gave the Middle-Upper Ordovician age, whereas one grain
presented age of 448.9 ± 8.4 Ma with a relatively low
232
Th/
238
U
ratio value (= 0.09). Nevertheless, this grain shows a growth
zoning even in internal texture, though slightly deformed.
The other two grains (455.8±9.1 and 464.0±8.7 Ma) display
characteristic features of magmatic origin, meaning oscilla-
tory growth zoning and
232
Th/
238
U ratio values of 0.52 and
0.66, respectively (Fig. 3c). Only one zircon grain gave
Fig. 7. a — Concordia plots of detrital zircons from the Hámor Fm., sample GZ-27. b — Corresponding PDP. c — Concordia plot for all dated
detrital zircon ages from the sample 29-LA. d — Selected sector for age spectrum from 300 to 900 Ma, with indication of the Concordia age.
e — Corresponding PDP diagram of all dated zircons from the sample 29-LA. f — PDP diagram of detrital zircon ages from the samples GZ-27
and 29-LA.
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Furongian age of 493.1± 9.4 Ma. Four other detrital zircon
grains presented the Precambrian ages, while three of them
yielded Tonian–Stenian of 901.0 ±16, 923.0 ±17 and
1201.0 ± 31 Ma and the other one a Paleoproterozoic age of
2222.0 ±12 Ma (Supplement, Table S2).
Thus, the main peak at 350 Ma, accompanied by two sub-
peaks at 301 and 456 Ma are emphasized on the PDP diagram
(Fig. 8).
Novoveská Huta Formation
A detrital zircon analysis from sample LA-66 was first pub-
lished in the article Vozárová et al. (2013). At present the set of
measurements has been completed by the additional data and
recalculated. Detrital zircon ages show a relatively good con-
cordance, 30 analysed concordant spots out of 33 (Supplement,
Table S2). The Concordia ages, calculated from the cluster
along the Concordia curve, show 294.2 ± 6.9 Ma (from seven
spots), 363.5 ± 4.5 (from ten spots) and 488.9 ± 8.2 Ma (from
five spots) (Fig. 9). The youngest detrital zircon ages are ran-
ging from 275.8±5.9 to 305.9±6.1 Ma. The magmatic origin
of this population is confirmed by the
232
Th/
238
U ratio values
ranging from 0.24 to 0.61 and a characteristic oscillatory
growth zoning. Upper Devonian to Mississippian ages ranging
from 352.7 ± 6.6 to 379.3 ±7.4 Ma are dominant. The majority
of this detrital zircons group is of magmatic origin, docu-
mented by
232
Th/
238
U ratios in the range of 0.10 –1.12, as well
as an oscillatory growth zoning. The only exception is spot 24,
determined on the rim of xenocrystic core, with 0.02 value of
232
Th/
238
U ratio, indicating the Mississippian/Famennian
metamorphic event (356.8 ± 6.7 Ma). Similarly, two spots in
the age of 471.3 ± 9.7 and 480.8 ± 9 Ma (Lower Ordovician)
were determined within the rims that mantled the strong
resorbed xenocrystic cores, with
232
Th/
238
U ratio of 0.08 and
0.02, respectively. Another three detrital zircon grains, ranging
from 513.0 ±10 to 495.3 ± 9.3 Ma ages (Upper Cambrian),
show the oscillatory zoned internal texture and
232
Th/
238
U
ratios between 0.21– 0.53 that confirm presumably acid mag-
matic sources. Precambrian detrital zircons are scarcely pre-
sented in the studied sample (5 grains). One of these, with
the age of 588.0 ±12 Ma belongs to the Ediacaran, another one
of 1502.2 ± 9.8 Ma to the Calymmian, and the last four zircons
are Paleoproterozoic–Neoarchean of 2314.0 ± 22, 2653.2 ± 4.2,
2697.3 ± 9.9 and 2725.0 ±15 Ma.
Whole zircon age spectrum from the sample LA-66 is
characterized on the PDP diagram by the dominant peak at
364 Ma, and smaller peaks at 301, 494 and 2655 Ma are
revealed (Fig. 9).
Discussion
The age distributions from previous (Vozárová et al. 2013)
and recent detrital zircon data are displayed as Kernel Density
Estimates (Fig. 10). The whole set of measurements of the
Mississippian Hrádok Fm. show the noticeable unimodal dis-
tribution with peak at 352 Ma (Fig. 10). The substantial part of
the whole studied detrital zircon population was derived from
magmatic sources, which is indicated by higher Th/U ratios,
ranging from 0.3 to >1. Only three analysed spots in the age of
340 ± 2, 356 ±7 and 368 ± 4 Ma, from the whole Famennian/
Tournaisian zircon assemblage, have typical features of meta-
morphic origin, with low Th/U ratio values (0.02–0.04) and
a weak or absent growth zoning. These spots represent meta-
morphic cores that are thinly rimmed by magmatic zircons,
Fig. 8. a — Concordia plot for all detrital zircons from the Petrova
Hora Fm., sample 74-LA. b — Selected Concordia for age spectrum
from 260 to 540 Ma, with indication of the Concordia ages.
c — Corresponding PDP.
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indicating a reworking during later stages of the Variscan mag-
matic cycle. Two metamorphic rims aged of 356 Ma and
565 Ma were found around the older detrital magmatic zircons
(2.43 Ga and 2.66 Ga, respectively). This clearly documents
the repeated recycling of the old zircon derived from the Paleo-
proterozoic/Neoarchean crust surpassing a strong Neopro-
terozoic and Variscan metamorphic overprint.
Detrital zircon age spectra reflect the tectonic setting of
the basin in which the studied sediments were deposited and
thus represent major phases of crust formation (Condie et al.
2009; Hawkesworth et al. 2010; Cawood et al. 2012). Large
volumes of magma are generated in convergent plate margin
settings. Convergent margin basins have a high proportion of
detrital igneous zircons (generally greater than 50 %) with
unimodal distribution. The crystallization ages are close to
the age of host sediments (Cawood et al. 2012). In fact,
the 370–344 Ma zircon ages include approximately 75 % from
the whole zircon age data of the Hrádok Fm. and the 352 Ma
peak age is nearly corresponding to its depositional age
(Tournaisian–Visean microfloral assemblages documented by
Bajaník & Planderová 1985).
Basins that contain a large number of igneous zircons with
ages close to the time of sediment accumulation reflect the
set ting of the magmatic activity (e.g., forearc, trench, and
backarc basins on convergent plate margins) (Dickinson &
Gehrels 2009; Condie et al. 2009; Cawood et al. 2012).
The presence of zircon grains with ages approximating to the
time of accumulation of the host sediments is likely to reflect
the proximity of the basin to a plate margin (Hawkesworth et
al. 2010). The NGU Mississippian metasedimentary rocks
have a unimodal detrital zircon population, which is similar to
the depositional age of the Hrádok Fm. The latter sedimentary
record shows the detrital zircons clustering within the 352 Ma
peak that indicates the main crystallization age of magmatites
in the supposed source area. Thus, this unimodal igneous zir-
con detritus reflects an extensive clastic input from a supposed
magmatic arc into the deep-slope Hrádok Fm. basin, situated
along an active margin, what is consistent with a convergent
margin setting.
Completely different detrital zircon distributions are dis-
played on the KDE plot from the Pennsylvanian Rudňany and
Hámor formations. The basal Rudňany Fm. shows a multi-
modal distribution, with the peaks at 357, 520, 667, 2021 and
2696 Ma (Fig. 10a). Similarly, detrital zircon populations from
the Hámor Fm. display main peaks at 335, 453 and 577 Ma on
the KDE plot (Fig. 10a). These patterns reflect the variable
amount of zircon detritus derived from the Tournaisian/
Famennian syn-collisional magmatism, as well as older ages,
reflecting units incorporated in the Variscan orogenic belt.
A relatively higher presence of the Cambrian–Ordovician and
the Ediacaran–Cryogenian zircon ages and increasing number
of the Paleoproterozoic–Neoarchean zircon grains are cha-
racteristic. These detrital zircon age spectra correspond to
an inconstant and mixed source area that is characteristic for
the collisional belt provenance (Dickinson & Gehrels 2009
and references therein). Based on Cawood et al.’s (2012) sedi-
mentary basins classification these originated in connection
with continental collision, such as foreland basins (collisional
basin type). While between the Pennsylvanian detrital zircon
populations the igneous zircon grains are predominant, some
of them indicate derivation from the metamorphic sources.
These are grouped into several time sections: Upper Devonian–
Mississippian in the range of 387–353 Ma, Lower and Upper
Fig. 9. a — Concordia plot of detrital zircons from the Novoveská
Huta Fm., sample LA-66 (old and new data together; old data taken
from Vozárová et al. 2013). b — Selected Concordia for age spec-
trum from 250 to 650 Ma, with indication of the Concordia ages.
c — Corresponding PDP.
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Ordovician aged from 476 to 451 Ma and Silurian, aged of 440
and 426 Ma (present paper and Vozárová et al. 2013).
The next group of selected detrital zircons was collected
from the Permian red-beds, at the Petrova Hora and Novoveská
Huta formations. Both formations reveal nearly similar age
peaks on the KDE plot, in the range of Lower/Middle
Ordovician (486 vs. 460 Ma) and Mississippian (356 vs.
350 Ma) (Fig. 10). Among detrital zircons the occurrences of
the Gzhelian–Asselian igneous zircons in the range from
306 ± 6 to 296 ± 6 Ma are exceptional. A small number of
Fig. 10. a — Kernel Density Estimation for the entire detrital zircon populations, with discordant filter of 10 %. b — Kernel Density Estimation
for the whole studied Carboniferous–Permian detrital zircon population with the corresponding PDP diagram. Note: In the diagrams have been
used all measurements, taken from the present data and the paper Vozárová et al. 2013.
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the Artinskian–Kungurian ages, ranging from 281± 6 to
276 ± 6 Ma were identified within the Novoveská Huta Fm.
zircon population. They represented reworked zircon grains
from the syn-sedimentary volcanic events. In general, the dis-
tribution of detrital zircons within both Permian formations
reproduce the post-collisional tectonic setting (extensional
basins in the sense of Cawood et al. 2012). Small number of
zircon ages close to the depositional age of the Permian sedi-
mentary formations (Artinskian–Kungurian) reflect a rift-
related magmatic activity.
The presented detrital zircon ages, with the main peaks at
300, 355, 455, 492, 562 and ~ 2.0 and ~ 2.7 Ga on the KDE
plot (Fig. 10b), specify generally, the provenance of the NGU
Carboniferous–Permian sediments from the Western Car pa-
thian Crystalline Basement (WCCB) crust and the pre-Carbo-
niferous complexes of the Northern Gemericum Basement.
As the latter complexes consist mainly of the zircon poor
rocks (metabasalt, amphibolite, metagabbro, serpentinite,
phyl lite), the studied detrital zircon population largely reflect
derivation from the WCCB crust. This contradicts the petro-
facial analysis of the lithic fragments within the NGU
Carboniferous–Permian sediments, containing detritus from
the NGU pre-Carboniferous complexes predominantly
(Vozárová 1973, 1996, 1998 a, b; Vozárová & Vozár 1988 and
references therein).
The large number of magmatic zircon data, ranging from
370 to 340 Ma, were published from the Tatricum and
Veporicum granitoids, which document the evidence of suc-
cessive I- to S-type granitic magmatism (Bibikova et al. 1988;
Kráľ et al. 1997; Poller & Todt 2000; Poller et al. 2000; Putiš
et al. 2003; Poller et al. 2005; Kohút et al. 2009; Burda et al.
2011, 2013; Broska et al. 2013; Gawęda et al. 2016). This time
interval includes pre-plate and late-orogenic/anatectic events
of magmatic activities of the Variscan orogeny. Second impor-
tant tectono–thermal events, which have been ascertained in
the NGU Carboniferous–Permian zircon assemblages are con-
centrated in the Cambrian–Ordovician time interval that is
well documented by detrital zircon ages, ranging from 520 to
453 Ma. This time span fits into the magmatic zircon ages
from the Layered Amphibolite Complex (LAC) and different
orthogneisses in the WCCB (Putiš et al. 2001, 2003, 2008,
2009a; Gaab et al. 2005, 2006). The Cambrian magmatic zir-
con ages (Supplement, Table S1; Fig. 5) were also ascertained
in the biotite–plagioclase orthogneiss cobble from the Penn-
sylvanian Rudňany Fm., with expressive metamorphic over-
print at 386 Ma in the zircon rims (present paper). This cobble
could be derived from the NGU Klátov Complex, in which
biotite–plagioclase gneisses are associated with the prevalent
amphibolites (Bajaník & Hovorka 1981; Hovorka et al. 1990;
Faryad 1986, 1990; Radvanec 1994). The oldest K/Ar radio-
metric data from the amphibolites gave 324–281 Ma meta-
morphic age (Kantor et al. 1981). The newest zircon data
yielded the magmatic Concordia age at 482 ± 9 Ma with indi-
cation of remelting at 383 ± 3 Ma (Putiš et al. 2009a).
In the studied detrital zircon population, metamorphic zir-
cons are scarce and had been noticed either as the rim around
the older magmatic cores or as the individual detrital grains.
They are concentrated into three-time intervals: i) Upper
Devo nian/Mississippian in the range of 387–353 Ma; ii) Lower
Ordovician in the range of 476–469 Ma; iii) Upper Ordovician–
Silurian in the range of 451–426 Ma (present paper and
Vozárová et al. 2013). Devonian–Mississippian metamorphic/
anatectic ages were described by U–Pb zircon data from
the WCCB different orthogneisses, migmatites, metagabbro
dolerites, layered amphibolites and leucosome layers in LAC,
metatonalites, as well as from metagabbro of the NGU zone
(Poller et al. 2000; Poller & Todt 2000; Putiš et al. 2003, 2008,
2009a; Gaab et al. 2005) and CHIME monazite ages from
WCCB gneisses and micaschists (Janák et al. 2004). These
metamorphic ages are mainly Variscan. A rare 430 Ma meta-
morphic age was described from the leucotonalite of LAC
complex (Putiš et al. 2008).
Generally, the Precambrian zircon ages are presented in
the very variable amounts (from 8 % to ~30 %). They are
relatively frequent in sedimentary formations deposited after
the sedimentation break (Rudňany, Hámor and Novoveská
Huta formations). Paleoproterozoic (Orosirian/Rhyacian) and
Neoarchean ages of 2.0 Ga and 2.5–2.7 Ga respectively pre-
dominate among the Precambrian zircons. This population is
well documented in the cobble from the Rudňany Fm. con-
glomerates (sample GZ-36A) with the main age peaks at 2028
and 2688 Ma and smaller peaks with Lower Cambrian/Late
Neoproterozoic ages at 537 and 576 Ma (Fig. 5). As the youn-
gest zircons are Lower Cambrian, the supposed age of this
quartzite rock could be Upper Cambrian/Ordovician which
corresponds well with the “Armorican Quartzite” lithofacies
(Henderson et al. 2016; Fernández-Suárez et al. 2002; Linneman
et al. 2004, 2014). In general, the Precambrian detrital zircon
population from the NGU Carboniferous–Permian sedimen-
tary rocks are concordant with the Smrečinka Fm. detrital zir-
con population, from the basal part of the Rakovec Group,
which is a part of the NGU Variscan basement (Vozárová et al.
2019). This dispersal of detrital zircon ages suggests a linkage
with Armorican terranes, which are characterized by deriva-
tion from the Cadomian arc that resides on the periphery of
the West African Craton of North Gondwana. Reworking of
the Eburnian crust (1.8–2.1 Ga) is characteristic. But, the recy-
cling of the small number of Tonian–Stenian (0.8–1.0 Ga) and
Grenvillean ages (1.2–1.5 Ga) were ascertained in detrital zir-
cons from the NGU Permian sequences. This zircon popu-
lation is not characteristic for the Armorican/West African
Craton provenance (e.g., Linnemann et al. 2007; Abati et al.
2012; Gärtner et al. 2013, 2016; Henderson et al. 2016).
Nevertheless, a small number of Mesoproterozoic ages were
also described from the Armorican Quartzites of the Canta-
brian Zone of NW Iberia (Fernández-Suárez et al. 2002;
Guttiérrez-Alonso et al. 2007), as well as from the Ordovician
sandstones of Corsica (Avigad et al. 2018). Perhaps, the pre-
sence of Mesoproterozoic zircons in the NGU Pennsylvanian–
Permian sequence, at least in small proportions, indicates
a possible presence of the pre-Neoproterozoic crustal vestiges
that were accreted within the Western Carpathian Variscan
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, 2019, 70, 6, 512–530
orogenic domain. Another possibility is the derivation from
the Southern Gemericum basement, in which Tonian–Stenian
zircon ages are relatively common, but the Grenvillean-aged
zircons are absent or their presence is negligible (Vozárová et
al. 2012, 2017). Equally, the presence of the Variscan mag-
matic zircons is the considerable difference between the NGU
Carboniferous–Permian and SGU Permian detrital zircon
populations. While in the NGU Carboniferous–Permian sedi-
ments these igneous zircons occur continuously in all forma-
tions, in the SGU Permian they are present only in the upper
lithostratigraphic unit (Štítnik Fm.; Vozárová et al. 2012). But
that would presume the large transform emplacement of the
SGU basement, in which it was incorporated into the Variscan
collisional belt in the Permian.
Conclusion
The detrital zircon age patterns of the Carboniferous–
Permian sedimentary basins in the Northern Gemericum were
controlled by tectonic settings, connected with the gradual
closing of the Variscan collisional suture.
The Mississippian detrital zircon population is characte-
rized by its unimodal distribution, with a sharp age peak at
352 Ma. Among those, the dominant portion is represented by
detrital zircons of igneous origin, with ages close to the depo-
sitional age of the host sediments, which is consistent with
a convergent plate margin setting. The Mississippian basin
reflects derivation from a magmatic arc that was nearly coeval
with accumulation of the sediments.
The Pennsylvanian detrital zircon population is distinctive
because of the multimodal distribution and increased amount
of Neoproterozoic and Neoarchean ages. This pattern reflects
the variable amount of zircon detritus from syn-collisional
magmatism (peaks at 335 and 357 Ma) and the pre-existing
magmatic rocks associated with opening of the Rakovec sedi-
mentary trough (from 453 to 520 Ma), as well as a band of
older ages (577–667 Ma and 2021–2696 Ma, respectively),
reflecting the units caught in the Variscan orogenic belt.
The Pennsylvanian basin was formed during continental colli-
sion, in the foreland setting.
Basically, the same trend in the distribution of detrital
zircons was also found in the Permian sediments. The only
difference is the presence of younger magmatic ages, from
Kasimovian/Gzhelian to Asselian (306–294 Ma) and Artin-
skian–Kungurian (280–276 Ma). This pattern reflects a post-
collisional, extensional type of sedimentary basin. Zircons
with ages close to the depositional age of the Permian forma-
tions reflect rift-related magmatic activity.
Acknowledgements: The financial support of the Slovak
Research and Development Agency (projects ID: APVV-
0546- 11 and APVV-0146-16) and of the Scientific Grant
Agency of the Ministry of Education of the Slovak Republic
and the Slovak Academy of Sciences (project VEGA
2/0006/19) is gratefully appreciated. The authors would like
to thank U. Klötzli and Z. Németh for constructive reviews
and for their helpful and critical comments which led to signi-
ficant improvement of an earlier versions of the manuscript.
References
Abati J., Aghzer A.M., Gerdes A. & Ennih N. 2012: Insights on the
crustal evolution of the West African Craton from Hf isotopes in
detrital zircons from Anti-Atlas belt. Precambrian Res. 212–213,
263–274.
Abonyi A. 1971: Stratigraphic and tectonic evolution of the Gemeric
Carboniferous west from the Štítnik Fault. Geol. Práce, Spr. 57,
339–348 (in Slovak).
Andrusov D. 1959: Geology of the Czechoslovak Western Carpa-
thians, 2
nd
part. VEDA Publishing House, Bratislava, 1–376
(in Slovak).
Avigad D., Rossi Ph., Gerdes A. & Abdo A. 2018: Cadomian metase-
diments and Ordovician sandstones from Corsica: detrital zircon
U–Pb–Hf constraints on their provenance and paleogeography.
Int. J. Earth Sci. (Geol. Rundsch.) 107, 2803–2818. https://doi.
org/10.1007/s00531-018-1629-3
Bajaník Š. & Hovorka D. 1981: The amphibolite facies metabasites of
the Rakovec Group of Gemericum (West Carpathians). Geol.
Zborn. Geol. Carpath. 32, 6, 679–705.
Bajaník Š., Vozárová A. & Reichwalder P. 1981: Lithostratigraphic
classification of Rakovec Group and Late Paleozoic sediments
in the Spišsko-gemerské rudohorie Mts. Geol. Práce, Spr. 75,
27–56 (in Slovak).
Bajaník Š., Hanzel V., Ivanička J., Mello J., Pristaš J., Reichwalder P.,
Snopko L, Vozár J. & Vozárová A. 1983: Explanation to geolo-
gical map of the Slovenské rudohorie Mts. – eastern part. D. Štúr
Inst. Geol. Publ. House, Bratislava, 3–223 (in Slovak with
English summary).
Bajaník Š., Ivanička J., Mello J., Pristaš J., Reichwalder P., Snopko L.,
Vozár J. & Vozárová A. 1984a: Geological map of the Slovenské
rudohorie Mts. – eastern part, 1:50 000. D. Štúr Inst. Geol.,
Bratislava.
Bajaník Š., Vozárová A., Snopková P. & Straka P. 1984b: Lithostrati-
graphy of the Črmeľ Group. Manuscript No. 58729, Archives
D. Š. Inst. Geology, Bratislava, 1–90 (in Slovak).
Bajaník Š. & Planderová E. 1985: Stratigraphic position of the lower
part of the Ochtiná Formation (between Magnezitovce and
Magura). Geol. Práce, Spr
. 82, 67–76 (in Slovak).
Bibikova E.V., Cambel B., Korikovsky S.P., Broska I., Gracheva T.V.,
Makarov V.A. & Arakeliants M.M. 1988: U–Pb and K–Ar iso-
topic dating of Sinec (Rimavica granites) (Kohút zone of Vepo-
rides). Geol. Zborn. Geol. Carpath. 39,147–157.
Biely A., Bezák V., Elečko M., Gross P., Kaličiak M., Konečný V.,
Lexa J., Mello J., Nemčok J., Potfaj M., Rakús M., Vass D.,
Vozár J. & Vozárová A. 1996a: Explanation to geological map of
Slovakia, 1:500 000. Dionýz Štúr Publisher, Bratislava, 1–76.
Biely A., Bezák V., Elečko M., Gross P., Kaličiak M., Konečný V.,
Lexa J., Mello J., Nemčok J., Potfaj M., Rakús M., Vass D.,
Vozár J. & Vozárová A. 1996b: Geological map of Slovakia:
Ministry Environm. Slovak Republic, Geol. Surv. Slovak
Republic, Bratislava.
Black L.P., Kamo S.L., Allen C.M., Aleinikoff J.N., Davis D.W.,
Korsch R.J. & Foudoulis C. 2003: TEMORA 1: a new zircon
standard for Phanerozoic U–Pb geochronology. Chem. Geol.
200, 155–170. https://doi.org/10.1016/S0009-2451(03)00165-7
Bouček B. & Přibyl A. 1960: Revision der Trilobiten aus dem slowa-
kischen Oberkarbon. Geol. Práce, Spr. 20, 5–50 (in Czech,
German summary).
528
VOZÁROVÁ, ŠARINOVÁ, LAURINC, LEPEKHINA, VOZÁR, RODIONOV and LVOV
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Broska I., Petrík I., Beʹeri-Shlevin Y., Majka J. & Bezák V. 2013:
Devonian/Mississippian I-type granitoids in the Western
Carpathians: A subduction-related hybrid magmatism. Lithos
162–163, 27–36.
Burda J., Gawęda A. & Klötzli U. 2011: Magma hybridization in
the Western Tatra Mts. granitoid intrusion (S-Poland, Western
Carpathians). Mineral. Petrol. 103, 1–4, 19–36.
Burda J, Gawęda A. & Klötzli U 2013: Geochronology and petroge-
nesis of granitoid rocks from the Goryczkowa Unit, Tatra Moun-
tains (Central Western Carpathians). Geol. Carpath. 64, 6,
419–435. https://doi.org/10.2478/geoca-2013-0029
Cawood P.A., Hawkesworth C.J. & Dhuime P. 2012: Detrital zircon
record and tectonic setting. Geology 40, 875–878. https://doi.
org/10.1130/G32945.1
Condie K.C., Belousova E., Griffin W.L. & Sircombe K.N. 2009:
Granitoid events in space and time: Constraints from igneous
and detrital zircon age spectra. Gondwana Res. 15, 228–242.
https://doi.org/10.1016/j.gr.2008.06.001
Dallmeyer R.D., Neubauer F., Handler R., Fritz H., Müller W.,
Pana D. & Putiš M. 1996: Tectonothermal evolution of the inter-
nal Alps and Carpathians: Evidence from
40
Ar/
39
Ar mineral and
whole rock data. Eclogae Geol. Helv. 89, 203–227.
Dallmeyer R.D., Németh Z. & Putiš M. 2005: Regional tectono-
thermal events in Gemericum and adjacent units (Western Car-
pathians, Slovakia): Contribution by
40
Ar/
39
Ar dating. Slovak
Geol. Mag. 11, 2–3, 155–163.
Dickinson W.R. & Gehrels G.E. 2009: Use of U–Pb ages of detrital
zircons to infer maximum depositional ages of strata: A test
against a Colorado Plateau Mesozoic database: Earth Planet.
Sci. Lett. 288, 115–125. https://doi.org/10.1016/j.epsl.2009.09.013.
Ebner F., Vozárová A., Kovács S., Kräutner H.-G., Krstić B.,
Szederkényi T., Jamićić D., Balen D., Belak M. & Trajanova M.
2008: Devonian-Carboniferous pre-flysch and flysch environ-
ments in the Circum Pannonian Region. Geol. Carpath. 59,
159–195.
Faryad S.W. 1986: Metamorphic evolution of paragneisses from
Klátov region (Gemericum). Geol. Zborn. Geol. Carpath. 39, 6,
729–749.
Faryad S.W. 1990: Gneiss–amphibolite complex of the Gemericum.
Miner. Slov. 22, 303–318.
Fernández-Suárez J., Gutiérrez-Alonso G. & Jeffries T.E. 2002:
The importance of along-margin terrane transport in northern
Gondwana: insights from detrital zircon parentage in Neopro-
terozoic rocks from Iberia and Brittany. Earth Planet. Sci. Lett.
204, 75–88.
Gaab A.S., Poller U., Janák M., Kohút M. & Todt W. 2005: Zircon
U–Pb geochronology and isotopic characterization for the
pre-Mesozoic basement of the Northern Veporic Unit (Central
Western Carpathians, Slovakia). Schweiz. Mineral. Petrogr. Mitt.
85, 69–88.
Gaab A.S., Janák M., Poller U. & Todt W. 2006: Alpine reworking of
Ordovician protoliths in the Western Carpathians: geochrono-
logical and geochemical data on the Muráň Gneiss complex.
Lithos 87, 261–275.
Gärtner A., Villeneuve M., Linnemann U., El Archi A. & Bellon H.
2013: An exotic terrane of Laurussian affinity in the Maureta-
nides and Souttoufides (Moroccan Sahara). Gondwana Res. 24,
687–699.
Gärtner A., Villeneuve M., Linnemann U., Gerdes A., Youbi N.,
Guillou O. & Rjimati E.-C. 2016: History of the West African
Neoproterozoic Ocean: key to the geotectonic history of circum-
Atlantic Peri-Gondwana (Adrar Souttouf Massif, Moroccan
Sahara). Gondwana Res. 29, 1, 220–233.
Gawęda A., Burda J., Klötzli U., Golonka J. & Szopa K. 2016:
Episodic construction of the Tatra granitoid intrusion (Central
Western Carpatians, Poland/Slovakia): consequences for the
geodynamics of Variscan collision and Rheic Ocean closure.
Int. J. Earth Sci. (Geol. Rundsch.) 105, 1153–1174. https://doi.
org/10.1007/s00531-015-1239-2
Grecula M. 1998: Carboniferous of the Črmelicum terrane, Western
Carpathians: relics of a fore-arc basin within Alpide Variscides.
Miner. Slov. 30, 109–136.
Gutiérrez-Alonso G., Fernández-Suárez J., Guttiérrez-Marco J.C.,
Corfu J. & Suárez M. 2007: U–Pb depositional age for the upper
Barrios Formation (Armorican Quartzite facies) in the Canta-
brian zone of Iberia: Implication for stratigraphic correlation and
paleogeography. In: Linnemann U., Nance R.D., Kraft P. &
Zulauf G. (Eds.): The evolution of Rheic Ocean: From Avalo-
nian–Cadomian Active margin to Alleghenian–Variscan Colli-
sion. Geol. Soc. Am., Spec. Pap. 423, 287–296.
Hawkesworth C. J., Dhuime B., Pietranik A., Cawood P., Kemp T. &
Storey C. 2010: The Generation and Evolution of the Continen-
tal Crust. J. Geol. Soc., London 167, 229–248. https://doi.org/
10.1144/0016-76492009-072
Henderson B.J., Collins W.J., Murphy J.B., Gutiérrez-Alonso G. &
Hand M. 2016: Gondwanan basement terranes of the Variscan
Appalachian orogen: Baltican, Saharan and West African haf-
nium isotopic fingerprints in Avalonia, Iberia and the Armorican
Terranes. Tectonophysics 681, 278–304.
Hiess J., Condon DJ., McLean N. & Noble SR. 2012:
238
U/
235
U sys-
tematics in terrestrial uranium-bearing minerals. Science 335,
1610–1614.
Hovorka D., Ivan P., Jilemnická I. & Spišiak J. 1988: Petrology
and geochemistry of metabasalts from Rakovec (Paleozoic of
Gemeric Unit, Inner Western Carpathians). Geol. Zborn. Geol.
Carpath. 39, 395–425.
Hovorka D., Ivan P. & Spišiak J. 1990: Lithology, Petrology, Meta-
morphism and Tectonic position of the Klátov Group (Paleozoic
of the Gemer unit, Inner Western Carpathians). Acta Geol.
Geogr. Univ. Comenianae, Geol. 45, 45–68.
International Commission on Stratigraphy. International Chrono-
stratigraphic Chart v 2018/08. http://www.stratigraphy.org/
ICSchart/ChronostratChart 2018-08.pdf
Ivan P. 1997: Rakovec and Zlatník Formations: two different relics of
the pre-Alpine back-arc basin crust in the Central Western
Carpathians. In: Grecula P., Hovorka D. & Putiš M. (Eds.): Geo-
logical Evolution of the Western Carpathians. Miner. Slov.,
Monograph, Bratislava, 281–288.
Ivan P. 2009: Early Palaeozoic basic volcanism of the Western Car-
pathians: geochemistry and geodynamic position. Acta Geol.
Univ. Comenianae, Monographic serie, Comenius University,
Bratislava, 7–110 (in Slovak).
Ivan P. & Méres Š. 2012: The Zlatník Group – Variscan ophiolites on
the northern border of the Gemeric Superunit (Western Carpa-
thians).
Miner. Slov. 44, 39–56.
Janák M., Konečný P., Siman P. & Holický I. 2004: A metamorphic
history from electron microprobe dating of monazite: Variscan
evolution of The Tatra Mountains. Geolines 17, 47–48.
Kantor J., Bajaník Š. & Hurný J. 1981: Radiometric dating of meta-
morphites of amphibolite facies from the Rudňany Deposits,
Spišsko-gemerské rudohorie Mts. Geol. Zborn. Geol. Carpath.
32, 335–344.
Kohút M., Uher P., Putiš M., Ondrejka M., Sergeev S., Larionov A. &
Paderin I. 2009: SHRIMP U–Th–Pb zircon dating of the grani-
toid massifs in the Malé Karpaty Mountains (Western Carpa-
thians): evidence of Meso-Hercynian successive S- to I-type
granitic magmatism. Geol. Carpath. 60, 5, 345–350.
Kohút M., Trubač J., Novotný L., Ackerman L., Demko R., Bartalský B.
& Erban V. 2013: Geology and Re-Os molybdenite geochrono-
logy of the Kuríšková U–Mo deposit (Western Carpathians,
Slovakia). J. Geosci. 58, 275–286. https://doi.org/10.3190/
jgeosci.150
529
ZIRCON GEOCHRONOLOGY FROM CARBONIFEROUS–PERMIAN SANDSTONES (WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Kozur H., Mock R. & Mostler H. 1976: Stratigraphische Neueinstu-
fung der Karbonatgesteine der unteren Schichtenfolgen von
Ochtiná (Slovakei) in das oberste Vise-Serpukhovian (Namur A).
Geol. Palaeont. Mitt. 6, l, 1–29.
Kozur H. & Mock R. 1977: Erster Nachweis von Conodonten im
Paleozoikum (Karbon) der Westkarpaten. Čas. pro miner. geol.
22, 3, 299–305.
Kráľ J., Hess J.C., Kober B. & Lippolt H.J. 1997:
207
Pb/
206
Pb and
40
Ar/
39
Ar data from plutonic rocks of the Strážovské vrchy Mts.
basement, Western Carpathians. In: Grecula P., Hovorka D. &
Putiš M. (Eds.): Geological evolution of the Western Carpa-
thians. Mineralia Slovaca – Monograph, Bratislava, 253–260.
Krist E. 1954: Bindt–Rudňany conglomerates, Carboniferous of the
northern part of the Slovenské Rudohorie Mts. Geol. Práce,
Zošit 36, Dionýz Štúr Inst. Geology, Bratislava, 77–107 (in
Slovak).
Lexa O., Schulmann K. & Ježek J. 2003: Cretaceous collision and
indentation in the West Carpathians: View based on structural
analysis and numerical modelling. Tectonics 22, 6, 1066. https://
doi.org/10.1029/2002TC001472
Linnemann U., McNaughton N.J., Romer R.L., Gehmlich M.,
Drost K. & Tonk C. 2004: West African provenance for Saxo-
Thuringia (Bohemian Massif): did Armorica ever leave pre-
Pangean Gondwana? U/Pb SHRIMP zircon evidence and Nd-
isotopic record. Int. J. Earth Sci. (Geol. Rundsch.) 93, 683–705.
Linnemann U., Gerdes A., Drost K. & Buschmann B. 2007: The con-
tinuum between Cadomian orogenesis and opening of the Rheic
Ocean: constraints of the LA-ICP-MS zircon dating and analy-
ses of plate-tectonic setting, Saxo–Thuringian zone, northeastern
Bohemian Massif, Germany. Geol. Soc. Am. Spec. Pap. 423,
61–96.
Linnemann U., Gerdes A., Hofmann M. & Marko L. 2014: The Cado-
mian Orogen: Neoproterozoic to Early Cambrian crustal growth
and orogenic zoning along the periphery of the West African
Craton – Constraints from U–Pb zircon ages and Hf isotopes
(Schwarzburg Antiform, Germany). Precambrian Res. 244,
236–278.
Ludwig K.R. 2005: SQUID 1.12 A Userʼs Manual. A Geochrono-
logical Toolkit for Microsoft Excel. Berkeley Geochronology
Centre Special Publication, 1–22. http://www.bgc.org/
klprogrammenu.html
Ludwig K.R. 2012: Userʼs Manual for Isoplot 3.75. A geochronolo-
gical Toolkit for Microsoft Excel. Berkeley Geochronology Cen-
tre Special Publication 5, 1–71. http://www.bgc.org/isoplot.html
Mamet B. & Mišík M. 2003: Marine Carboniferous algae from meta-
carbonates of Ochtiná Formation (Gemeric Unit, Western Car-
pathians). Geol. Carpath. 54, 3–8.
Michalík J. (Ed.) 2007: Stratigraphic manual. Slovak stratigraphic
terminology, stratigraphic classification and method. VEDA,
Slovak Academy of Sciences, Bratislava, 1–166 (in Slovak).
Němejc F. 1947 Contribution to knowledge of floral remnants and
stratigraphical division of Permo-Carboniferous of Slovakia.
Rozpravy II. Čes. Akad. Věd 56, 15, Praha, 1–34 (in Czech).
Németh Z. 2002: Variscan suture zone in Gemericum: Contribution to
reconstruction of geodynamic evolution and metallogenic events
of Inner Western Carpathians. Slovak Geol. Mag. 8, 247–257.
Németh Z., Procházka W., Radvanec M., Kováčik M., Madarás J.,
Koděra P. & Hraško Ľ. 2004: Magnesite and talc origin in the
sequence of geodynamic events in Veporicum, Inner Western
Carpathians. Acta Petrol. Sinica 20, 837–854.
Novotný L. & Miháľ F. 1987: New lithostratigraphic units of the
Krompachy Group. Miner. Slov. 19, 97–113 (in Slovak).
Novotná N., Jeřábek P., Pitra P., Lexa O. & Racek M. 2015: Repeated
slip along a major decoupling horizon between crustal scale
nappes of the Central Western Carpathians documented in the
Ochtiná tectonic mélange. Tectonophysics 646, 50–64.
Neubauer F. & Vozárová A. 1990: The Noetsch-Veitsch-Northgemer-
ic Zone of Alps and Carpathians: Correlation, paleogeography
and significance for Variscan orogeny. In: Minaříková D. &
Lobitzer H. (Eds.): Thirty years of geological cooperation bet-
ween Austria and Czechoslovakia. Federal Geol. Surv., Vienna,
167–171.
Planderová E. & Vozárová A. 1982: Biostratigraphical correlation of
the Late Paleozoic formations in the West Carpathians. In: Sassi
F.P. (Ed.): Newsletter No. 4, IGCP Project No. 5, Padova, 67–71.
Plašienka D., Grecula P., Putiš M., Kováč M. & Hovorka D. 1997:
Evolution and structure of the Western Carpathians: an over-
view. In: Grecula P., Hovorka D., Putiš M. (Eds.): Geological
evolution of the Western Carpathians. Miner. Slov, Monograph,
Bratislava, 1–24
Plašienka D. 2018: Continuity and episodicity in the early Alpine tec-
tonic evolution of the Western Carpathians: How large-scale
processes are expressed by the orogenic architecture and rock
record data. Tectonics 37, 2029–2079. https://doi.org/
10.1029/2017TC004779
Poller U. & Todt W. 2000: U–Pb single zircon data of granitoids from
the High Tatra Mountains (Slovakia): implications for the geo-
dynamic evolution. Geol. Soc. Am. Spec. Pap. 350, 235–243.
Poller U., Janák M., Kohút M. & Todt W. 2000: Early Variscan mag-
matism in the Western Carpathians: U–Pb zircon data from gra-
nitoids and orthogneisses of the Tatra Mountains (Slovakia).
Int. J. Earth Sci. (Geol. Rundsch.) 89, 2, 336–349. https://doi.
org/10.1007/s005310000082
Poller U., Kohút M., Anders B. & Todt W. 2005: Multistage geochro-
nological evolution of the Veľká Fatra Mts. – a combined TIMS
and ion-microprobe study on zircons. Lithos 82, 113–124.
Putiš M., Kotov A.B., Korikovsky S.P., Salnikova E.B., Yakovleva
S.Z., Berezhnaya N.G., Kovach V.P. & Plotkina J.V. 2001: U–Pb
zircon ages of dioritic and trondhjemitic rocks from a layered
amphibolitic complex crosscut by granite veins (Veporic base-
ment, Western Carpathians). Geol. Carpath. 52, 1, 49–60.
Putiš M., Kotov A. B., Petrík I., Korikovsky S. P., Madarás J.,
Salnikova E.B., Yakovleva S.Z., Berezhnaya N.G., Plotkina
Y.V., Kovach V.P., Lupták B. & Majdán M. 2003: Early– vs. Late
orogenic granitoids relationships in the Variscan basement of
the Western Carpathians. Geol. Carpath. 54, 163–174.
Putiš M., Sergeev S., Ondrejka M., Larionov A., Siman P., Spišiak J.,
Uher P. & Paderin I. 2008: Cambrian–Ordovician metaigneous
rocks associated with Cadomian fragments in the West-Carpa-
thian basement dated by SHRIMP on zircons: a record from the
Gondwana active margin setting. Geol. Carpath. 59, 1, 3–18.
Putiš M., Ivan P., Kohút M., Spišiak J., Siman P., Radvanec M., Uher
P., Sergeev S., Larionov A., Méreš Š., Demko R. & Ondrejka M.
2009a: Meta-igneous rocks of the West-Carpathian basement,
Slovakia: indicators of Early Paleozoic extension and shortening
events. Bull. Soc. Géol. Fr. 180, 6, 461–471.
Putiš M., Frank W., Plašienka D., Siman P., Sulák M. & Biroň A.
2009b: Progradation of the Alpidic Central Western Carpathians
orogenic wedge related to two subductions: constrained by
40
Ar/
39
Ar ages of white micas. Geodyn. Acta 22, 1–3, 31–56.
Radvanec M. 1994: Petrology of the Gemeric gneiss-amphibolite com-
plex, northern part of the Rudňany deposits. Part I: P–T–x condi-
tions and zonality of metamorphism. Miner. Slov. 26, 223–238.
Radvanec M., Németh Z., Kráľ J. & Pramuka S. 2017: Variscan
dismembered metaophiolite suite fragments of Paleo-Tethys in
Gemeric unit, Western Carpathians. Miner. Slov. 49, 1–48.
Rakusz Gy. 1932: Die oberkarbonischen Fosilien von Dobšiná und
Nagyvisnyó. Geol. Hungarica, serie Paleont. 8, 1–219.
Rakús M., Potfaj M. & Vozárová A. 1998: Basic paleogeographic and
paleotectonic units of the Western Carpathians. In: Rakús M.
(Ed.): Geodynamic development of the Western Carpathians.
D. Štúr Publ., Bratislava, 15–26.
530
VOZÁROVÁ, ŠARINOVÁ, LAURINC, LEPEKHINA, VOZÁR, RODIONOV and LVOV
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Rojkovič I. & Konečný P. 2005: Th–U–Pb dating of monazite from
the Cretaceous uranium vein mineralization in the Permian rocks
of the Western Carpathians. Geol. Carpath. 56, 493–502.
Rojkovič I. & Miháľ F. 1991: Geological structure and uranium mine-
ralization in Permian of the north-eastern part of the Slovenské
Rudohorie Mts. Miner. Slov. 23, 123–132 (in Slovak with English
summary).
Rojkovič I. & Vozár J. 1972: Contribution to the relationship of the
Permian volcanism in the northern Gemerides and Choč Unit.
Geol. Zborn. Geol. Carpath. 23, Bratislava, 87–98.
Spišiak J., Hovorka D. & Ivan P. 1985: Klátov Group the representa-
tive of the Paleozoic amphibolite facies metamorphites of the
Inner Western Carpathians. Geol. Práce, Spr. 82, 205–220 (in
Slovak with English summary).
Steiger R.H. & Jäger E. 1977: Subcommission on geochronology:
Convention on the use of decay constants in geo- and cosmo-
chronology. Earth Planet. Sci. Lett. 36, 359–362.
Václav J. & Vozárová A. 1978: Characteristic of the Northern Geme-
ride Permian at Košická Belá. Záp. Karpaty, Sér. Min. Petr. Geo-
chem. Metalog. 5, 83–108 (in Slovak).
Vermeesch P. 2012: On the visualization detrital age distributions.
Chem. Geol. 312–313, 190–194. https://doi.org/10.1016/
j.chemgeo.2012.04.021
Vozárová A. 1973: Pebble analysis of the late Paleozoic conglome-
rates in Spišsko-Gemerské rudohorie Mts. Geol. Zborn. Západné
Karpaty 18, 7–98 (in Slovak).
Vozárová A. 1996: Tectono-sedimentary evolution of Late Paleozoic
basins based on interpretation of lithostratigraphic data (Western
Carpathians; Slovakia). Slovak Geol. Mag. 3–4, 251–271.
Vozárová A. 1997: Upper Permian-Lower Triassic evaporites in the
Western Carpathians (Slovakia). Slovak Geol. Mag. 3, 223–230.
Vozárová A. 1998a: Late Hercynian development in the Central Wes-
tern Carpathians. In: Rakús M. (Ed.): Geodynamic development
of the Western Carpathians. Geol. Surv. Slovak Rep., Dionýz Štúr
Publishers, 41–46.
Vozárová A. 1998b: Late Hercynian development in the Inner Wes-
tern Carpathians. In: Rakús M. (Ed.): Geodynamic development
of the Western Carpathians. Geol. Surv. Slovak Rep., Dionýz Štúr
Publishers, 75–80.
Vozárová A. 2001: Plagiogranite pebbles in Westphalian conglome-
rates of the Northern Gemericum Unit: their characteristic and
geotectonic significance (Western Carpathians). Krystalinikum
27, 79–88.
Vozárová A. & Vozár J. 1988: Late Paleozoic in West Carpathians.
Monogr., D. Štúr. Inst. Geol., Bratislava, 1–314.
Vozárová A., Frank W., Kráľ J. & Vozár J. 2005:
40
Ar/
39
Ar dating
of detrital mica from the Upper Paleozoic sandstones in
the Wes tern Carpathians (Slovakia). Geol. Carpath. 56, 6,
463–472.
Vozárová A., Šarinová K., Rodionov N., Laurinc D., Paderin I.,
Sergeev S. & Lepekhina E. 2012: U–Pb ages of detrital zircons
from Paleozoic metasandstones of the Gelnica Terrane (Southern
Gemeric Unit, Western Carpathians, Slovakia): evidence for
Avalonian–Amazonian provenance. Int. J. Earth Sci. (Geol.
Rundsch.) 101, 919–936. https://doi.org/10.1007/s00531-011-
0705-8
Vozárová A., Laurinc D., Šarinová K., Larionov A., Presnyakov S.,
Rodionov N. & Paderin I. 2013: Pb ages of detrital zircons in
relation to geodynamic evolution: Paleozoic of the Northern
Gemericum (Western Carpathians, Slovakia). J. Sediment. Res.
83, 915–927. https://doi.org/10.2110/jsr.2013.66
Vozárová A., Presnyakov S., Šarinová K. & Šmelko M. 2015: First
evidence for Permian-Triassic boundary volcanism in the Nor-
thern Gemericum: geochemistry and U-Pb zircon geochrono-
logy. Geol. Carpath. 66, 5, 375–391.
Vozárová A., Rodionov N., Šarinová K. & Presnyakov S. 2017: New
zircon ages on the Cambrian–Ordovician volcanism of the
Southern Gemericum basement (Western Carpathians, Slova-
kia): SHRIMP dating, geochemistry and provenance. Int. J.
Earth Sci. (Geol. Rundsch.) 106, 2147–2170. https://doi.
org/10.1007/s00531-016-1420-2
Vozárová A., Rodionov N. & Šarinová K. 2019: Recycling of Paleo-
proterozoic and Neoproterozoic crust recorded in Lower Paleo-
zoic metasandstones (Western Carpathians, Slovakia): evidence
from detrital zircons. Geol. Carpath. 70, 298–310.
Wiedenbeck M., Allé P., Corfu F., Griffin W.L., Meier M., Oberli F.,
von Quadt A., Roddick J.C. & Spiegel W. 1995: Three natural
zircon standards for U–Th–Pb, Lu–Hf, trace element and REE
analyses. Geostand. Newslett. 19, 1–23.
Williams I.S. 1998: U–Th–Pb geochronology by ion microprobe.
In: McKissen M.A., Shanks III W.C. & Ridley W.S. (Eds.):
Applications of microanalytical techniques to understanding
mineralizing processes. Rev. Econ. Geol. 7, 1–35.
Zágoršek K. & Macko A. 1994: Carboniferous Bryozoa from the
Jedlovec quarry in Ochtiná Formation (Gemericum, Western
Carpathians): Miner. Slov. 26, 5, 335–346.
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ZIRCON GEOCHRONOLOGY FROM CARBONIFEROUS–PERMIAN SANDSTONES (WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Plagioclase
Garnet
No
16 / 1
17 / 1
19 / 1
21 / 1
23 / 1
No.
18 / 1
20 / 1
22 / 1
Sample
GZ-55
GZ-55
GZ-55
GZ-55
GZ-55
Sample
GZ-55
GZ-55
GZ-55
Mineral
pl
pl
pl
pl
pl
Mineral
grt
grt
grt
Ana No.
an1
an2
an4
an6
an8
Ana No.
an3
an5
an7
SiO2
62.94
62.86
63.63
62.16
62.57
SiO2
38.06
37.80
37.79
Al2O3
23.54
22.63
22.24
23.10
23.36
TiO2
0.01
0.00
0.00
FeO
0.05
0.00
0.01
0.02
0.00
Al2O3
21.11
21.11
21.04
CaO
5.33
4.72
4.34
5.32
5.17
Cr2O3
0.03
0.01
0.01
Na2O
8.41
8.84
8.96
8.21
8.44
MgO
2.20
2.15
2.16
K2O
0.18
0.08
0.22
0.20
0.06
FeO
31.63
32.22
32.48
SrO
0.05
0.04
0.00
0.05
0.03
MnO
1.98
2.15
2.43
Total
100.50
99.17
99.41
99.06
99.63
CaO
6.38
5.61
5.22
apfu (8 oxygen)
Na2O
0.04
0.00
0.03
Si
2.774
2.803
2.827
2.778
2.778
Total
101.43
101.06
101.16
Al
1.223
1.189
1.165
1.217
1.222
apfu (8 cations)
Fe
0.002
0.000
0.000
0.001
0.000
Si
3.007
3.004
3.003
Ca
0.252
0.225
0.206
0.255
0.246
Tetr. Al
0.000
0.000
0.000
Sr
0.001
0.001
0.000
0.001
0.001
sum T
3.007
3.004
3.003
Na
0.719
0.764
0.772
0.711
0.727
Fe3+
0.033
0.021
0.029
K
0.010
0.005
0.012
0.012
0.003
Oct. Al
1.965
1.978
1.971
SUM
4.980
4.987
4.983
4.975
4.977
Cr
0.002
0.001
0.001
endmembers (%)
Ti
0.000
0.000
0.000
Or
1.05
0.48
1.26
1.18
0.34
sum X
2.000
2.000
2.000
Ab
73.29
76.84
77.91
72.75
74.47
Fe2+
2.056
2.119
2.129
An
25.66
22.69
20.84
26.06
25.19
Ca
0.540
0.478
0.444
Mg
0.259
0.255
0.256
Mn
0.132
0.145
0.164
Na
0.006
0.000
0.004
sum Y
2.993
2.996
2.997
endmembers (%)
Prp
8.67
8.50
8.55
Sps
4.43
4.83
5.48
Alm
68.81
70.72
71.13
Adr
1.64
1.07
1.45
Grs
16.44
14.87
13.40
Table S1: Microprobe analyses of plagioclases and garnets from the sample GZ-55.
Supplement
ii
VOZÁROVÁ, ŠARINOVÁ, LAURINC, LEPEKHINA, VOZÁR, RODIONOV and LVOV
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Hrádok Fm.
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th/
238
U
ppm
206
Pb*
(1)
206
Pb/
238
U
Age
±1s
err
(1)
207
Pb/
206
Pb
Age
±1s
err
%
Discordant
(1)
238
U/
206
Pb
*
±%
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
*
/
235
U ±%
(1)
206
Pb
*
/
238
U ±%
err
corr
GZ-28.1.1
0.46
130
120
0.95
6.6
367
4
297
130
−19
17.08
1.2
0.0523
5.7
0.42
5.8
0.0585
1.2
0.207
GZ-28.2.1
0.24
76
51
0.69
25.2
2087
19
2045
27
−2
2.61
1.1
0.1262
1.6
6.65
1.9
0.3822
1.1
0.561
GZ-28.3.1
0.00
238
82
0.36
16.4
496
4
555
48
12
12.50
0.9
0.0587
2.2
0.65
2.4
0.0800
0.9
0.363
GZ-28.4.1
0.34
173
49
0.29
11.6
482
5
444
84
−8
12.89
1.0
0.0558
3.8
0.60
3.9
0.0776
1.0
0.253
GZ-28.5.1
0.45
123
5
0.04
6.2
368
4
256
131
−31
17.00
1.2
0.0513
5.7
0.42
5.8
0.0588
1.2
0.206
GZ-28.6.1
0.53
150
42
0.29
10.4
498
5
474
117
−5
12.45
1.0
0.0566
5.3
0.63
5.4
0.0803
1.0
0.193
GZ-28.7.1
0.21
795
13
0.02
37.0
340
2
332
55
−2
18.48
0.7
0.0531
2.4
0.40
2.5
0.0541
0.7
0.262
GZ-28.8.1
0.28
706
273
0.40
32.0
330
2
308
62
−7
19.02
0.8
0.0525
2.7
0.38
2.8
0.0526
0.8
0.272
GZ-28.9.1
0.56
120
80
0.68
9.5
566
6
483
122
−15
10.89
1.1
0.0568
5.5
0.72
5.6
0.0918
1.1
0.193
GZ-28.10.1
0.17
227
65
0.30
15.5
492
4
403
54
−18
12.61
0.9
0.0548
2.4
0.60
2.6
0.0793
0.9
0.347
GZ-28.11.1
0.16
315
99
0.32
21.1
483
4
527
52
9
12.86
0.8
0.0579
2.4
0.62
2.5
0.0778
0.8
0.325
GZ-28.12.1
0.66
194
16
0.09
13.5
499
4
354
124
−29
12.42
0.9
0.0536
5.5
0.59
5.6
0.0805
0.9
0.159
GZ-28.13.1
0.60
87
33
0.39
6.2
509
6
439
143
−14
12.18
1.2
0.0557
6.4
0.63
6.5
0.0821
1.2
0.178
GZ-28.14.1
0.05
212
270
1.31
93.9
2678
15
2760
8
3
1.94
0.7
0.1921
0.5
13.64
0.8
0.5151
0.7
0.801
GZ-28.15.1
0.11
200
94
0.49
90.1
2717
16
2694
13
−1
1.91
0.7
0.1846
0.8
13.34
1.0
0.5243
0.7
0.687
GZ-28.16.1
-0.01
616
831
1.39
273.5
2685
14
2695
7
0
1.94
0.6
0.1847
0.4
13.15
0.8
0.5165
0.6
0.843
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
Error in Standard calibration was 0.4 % (not included in above errors but required when comparing data from different mounts).
(1) Common Pb corrected using measured
204
Pb.
Table S2: New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken from
Vozárová et al. 2013, are shaded.
iii
ZIRCON GEOCHRONOLOGY FROM CARBONIFEROUS–PERMIAN SANDSTONES (WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Table S2 (continued): New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken
from Vozárová et al. 2013, are shaded.
Rudňany Fm.
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th
/
238
U
ppm
206
Pb*
(1)
206
Pb/
238
U
Age
(1)
207
Pb/
206
Pb
Age
%
Discordant
(1)
238
U/
206
Pb
*
±%
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
*
/
235
U ±%
(1)
206
Pb
*
/
238
U ±%
err
corr
GZ-35_1.1
0.00
59
45
0.79
6.57
781.00
±13
832.00
±54
7
7.76
1.8
0.0668
2.6
1.19
3.2
0.1288
1.8
0.564
GZ-35_2.1
0.11
309
136
0.45
14.90
350.80
±5,2
354.00
±40
1
17.88
1.5
0.0536
1.8
0.41
2.3
0.0559
1.5
0.653
GZ-35_3.1
0.08
284
101
0.37
13.80
355.30
±5,3
364.00
±44
3
17.65
1.5
0.0538
2.0
0.42
2.5
0.0567
1.5
0.619
GZ-35_4.1
0.11
266
161
0.63
13.00
357.30
±5,4
371.00
±42
4
17.55
1.5
0.0540
1.9
0.42
2.4
0.0570
1.5
0.635
GZ-35_5.1
0.17
603
174
0.30
29.40
355.10
±5,2
347.00
±32
−2
17.66
1.5
0.0534
1.4
0.42
2.1
0.0566
1.5
0.725
GZ-35_6.1
0.10
250
472
1.95
23.60
671.70
±9,7
637.00
±30
−5
9.11
1.5
0.0609
1.4
0.92
2.1
0.1098
1.5
0.736
GZ-35_7.1
0.15
141
115
0.84
6.88
354.20
±5,6
340.00
±66
−4
17.70
1.6
0.0533
2.9
0.42
3.3
0.0565
1.6
0.482
GZ-35_8.1
0.07
365
3
0.01
104.00
1849.00
±24
2027.90
±8,2
10
3.01
1.5
0.1249
0.5
5.72
1.6
0.3322
1.5
0.955
GZ-35_9.1
0.06
446
169
0.39
200.00
2709.00
±33
2681.00
±15
−1
1.91
1.5
0.1831
0.9
13.19
1.7
0.5224
1.5
0.856
GZ-35_10.1
0.24
75
52
0.71
7.71
724.00
±12
698.00
±68
−4
8.41
1.7
0.0627
3.2
1.03
3.6
0.1189
1.7
0.467
GZ-35_11.1
0.01
249
252
1.04
130.00
3052.00
±37
2998.00
±16
−2
1.65
1.5
0.2224
1.0
18.57
1.8
0.6056
1.5
0.835
GZ-35_12.1
0.11
355
252
0.73
17.70
363.90
±5,4
330.00
±38
−9
17.22
1.5
0.0530
1.7
0.42
2.3
0.0581
1.5
0.672
GZ-35_13.1
0.06
175
54
0.32
74.60
2598.00
±32
2619.50
±8,3
1
2.01
1.5
0.1764
0.5
12.07
1.6
0.4963
1.5
0.949
GZ-35_14.1
0.03
761
224
0.30
237.00
1991.00
±25
2665.70
±9,7
34
2.76
1.5
0.1814
0.6
9.05
1.6
0.3618
1.5
0.927
GZ-35_15.1
0.04
724
248
0.35
38.20
384.10
±5,5
399.00
±24
4
16.29
1.5
0.0547
1.1
0.46
1.8
0.0614
1.5
0.805
GZ-35_16.1
0.26
166
44
0.27
11.50
497.10
±7,7
433.00
±64
−13
12.47
1.6
0.0555
2.9
0.61
3.3
0.0802
1.6
0.493
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
Error in Standard calibration was 0.51 %
(1) Common Pb corrected using measured
204
Pb.
iv
VOZÁROVÁ, ŠARINOVÁ, LAURINC, LEPEKHINA, VOZÁR, RODIONOV and LVOV
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Table S2 (continued): New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken
from Vozárová et al. 2013, are shaded.
Rudňany Fm. – metasandstone pebble
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th/
238
U
ppm
206
Pb*
(1)
206
Pb/
238
U
Age
±1s
err
(1)
207
Pb/
206
Pb
Age
±1s
err
%
Discordant
(1)
238
U/
206
Pb
*
±%
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
*
/
235
U ±%
(1)
206
Pb
*
/
238
U ±%
err
corr
GZ-36A.1.1
0.06
233
92
0.41
96.1
2529
16
2561
11
1
2.08
0.8
0.1703
0.7
11.28
1.0
0.4805
0.8
0.757
GZ-36A.2.1
0.13
66
27
0.43
20.8
2022
21
2034
31
1
2.71
1.2
0.1254
1.8
6.37
2.2
0.3684
1.2
0.563
GZ-36A.3.1
0.08
62
23
0.38
31.8
3000
36
2941
22
−2
1.69
1.5
0.2147
1.4
17.54
2.0
0.5925
1.5
0.735
GZ-36A.4.1
0.19
201
16
0.08
62.8
1996
14
2007
18
1
2.75
0.8
0.1235
1.0
6.18
1.3
0.3629
0.8
0.615
GZ-36A.5.1
0.37
66
36
0.56
22.2
2119
23
2060
32
−3
2.57
1.3
0.1272
1.8
6.83
2.2
0.3891
1.3
0.573
GZ-36A.6.1
0.15
294
120
0.42
90.3
1965
13
2025
14
3
2.80
0.8
0.1248
0.8
6.13
1.1
0.3564
0.8
0.708
GZ-36A.7.1
0.03
402
236
0.61
181.4
2720
14
2706
7
−1
1.90
0.6
0.1858
0.4
13.45
0.8
0.5250
0.6
0.832
GZ-36A.8.1
0.12
85
17
0.21
28.0
2082
22
2013
35
−3
2.62
1.3
0.1239
2.0
6.51
2.3
0.3811
1.3
0.537
GZ-36A.9.1
0.46
157
214
1.41
12.7
576
5
569
83
−1
10.70
1.0
0.0591
3.8
0.76
3.9
0.0934
1.0
0.245
GZ-36A.10.1
0.14
144
88
0.63
41.8
1874
13
1882
28
0
2.96
0.8
0.1151
1.5
5.36
1.7
0.3375
0.8
0.464
GZ-36A.11.1
0.12
194
56
0.30
87.6
2718
16
2706
10
0
1.91
0.7
0.1859
0.6
13.44
0.9
0.5244
0.7
0.747
GZ-36A.12.1
0.27
105
74
0.73
7.9
537
6
489
92
−9
11.50
1.1
0.0569
4.2
0.68
4.3
0.0869
1.1
0.249
GZ-36A.13.1
0.07
316
55
0.18
141.5
2700
14
2737
14
1
1.92
0.6
0.1894
0.8
13.58
1.0
0.5201
0.6
0.591
GZ-36A.14.1
0.04
170
207
1.25
73.6
2626
17
2770
11
5
1.99
0.8
0.1932
0.7
13.39
1.0
0.5027
0.8
0.765
GZ-36A.15.1
0.06
214
92
0.44
72.2
2134
12
2136
13
0
2.55
0.7
0.1328
0.8
7.19
1.0
0.3923
0.7
0.659
GZ-36A.16.1
-0.01
626
106
0.17
280.4
2705
13
2688
5
−1
1.92
0.6
0.1838
0.3
13.21
0.7
0.5213
0.6
0.891
GZ-36A.17.1
0.12
210
70
0.34
87.3
2543
14
2514
24
−1
2.07
0.7
0.1657
1.4
11.05
1.6
0.4837
0.7
0.426
GZ-36A.18.1
-0.01
836
164
0.20
361.7
2630
19
2834
20
8
1.99
0.9
0.2010
1.2
13.96
1.5
0.5037
0.9
0.592
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
Error in Standard calibration was 0.4 % (not included in above errors but required when comparing data from different mounts).
(1) Common Pb corrected using measured
204
Pb.
v
ZIRCON GEOCHRONOLOGY FROM CARBONIFEROUS–PERMIAN SANDSTONES (WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Table S2 (continued): New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken
from Vozárová et al. 2013, are shaded.
Rudňany Fm. – gneiss pebble
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th/
238
U
ppm
206
Pb*
(1)
206
Pb/
238
U
Age
(1)
207
Pb/
206
Pb
Age
%
Discordant
(1)
238
U/
206
Pb
*
±%
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
*
/
235
U ±%
(1)
206
Pb
*
/
238
U
±%
err
corr
GZ55_1.1
0.23
383
89
0.24
28.50
534.20
±2,5
552.00
±37
3
11.57
0.49
0.0586
1.70
0.70
1.80
0.0864
0.49
0.276
GZ55_1.2
1.48
68
4
0.06
3.65
385.70
±6,3
530.00
±400
37
16.21
1.70
0.0580
18.00
0.49
18.00
0.0617
1.70
0.093
GZ55_2.1
0.25
271
26
0.10
18.50
491.60
±3,8
456.00
±46
−7
12.62
0.80
0.0561
2.10
0.61
2.20
0.0792
0.80
0.358
GZ55_3.1
0.12
710
137
0.20
50.70
513.70
±1,9
517.00
±43
1
12.06
0.38
0.0577
2.00
0.66
2.00
0.0829
0.38
0.191
GZ55_4.1
0.17
460
87
0.20
33.30
521.00
±2,3
486.00
±36
−7
11.88
0.47
0.0569
1.60
0.66
1.70
0.0842
0.47
0.278
GZ55_5.1
0.08
1332
346
0.27
94.20
509.60
±1,5
512.00
±18
0
12.16
0.31
0.0575
0.80
0.65
0.86
0.0823
0.31
0.358
GZ55_6.1
0.12
1084
81
0.08
75.90
504.40
±1,6
510.00
±20
1
12.29
0.33
0.0575
0.92
0.65
0.98
0.0814
0.33
0.339
GZ55_6.2
0.77
71
0
0.01
3.82
386.70
±4,9
464.00
±130
20
16.17
1.30
0.0563
5.80
0.48
5.90
0.0618
1.30
0.221
GZ55_7.1
0.03
1840
695
0.39
132.00
518.00
±1,4
538.00
±13
4
11.95
0.28
0.0582
0.60
0.67
0.66
0.0837
0.28
0.424
GZ55_8.1
0.08
1352
442
0.34
98.30
523.40
±2,3
516.00
±19
−1
11.82
0.46
0.0576
0.87
0.67
0.99
0.0846
0.46
0.467
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
Error in Standard calibration was 0.36 % (not included in above errors but required when comparing data from different mounts).
(1) Common Pb corrected using measured
204
Pb.
vi
VOZÁROVÁ, ŠARINOVÁ, LAURINC, LEPEKHINA, VOZÁR, RODIONOV and LVOV
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Table S2 (continued): New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken from Vozárová et
al. 2013, are shaded.
Hámor Fm.
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th/
238
U ppm
206
Pb*
(1)
206
Pb/
238
U
Age
(2)
206
Pb/
238
U
Age
(3)
206
Pb/
238
U
Age
(1)
207
Pb/
206
Pb
Age
%
Discordant
Total
238
U/
206
Pb ±%
Total
207
Pb/
206
Pb ±%
(1)
238
U/
206
Pb
*
±%
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
*
/
235
U ±%
(1)
206
Pb
*
/
238
U ±%
err
corr
29LA.1.1 0.23
308
337
1.13
24.0
558.4 ±9,2
559.2 ±9,4
560.0
±11
516
±36
−8
11.03 1.70
0.0595 1.20
11.05
1.70
0.0577
1.60
0.72
2.40
0.0905
1.70 0.727
29LA.2.1 0.26
508
187
0.38
24.1
346.2 ±5,8
346.8 ±5,9
346.3 6.30
287
±49
−17
18.08 1.70
0.0542 1.50
18.13
1.70
0.0520
2.20
0.40
2.80
0.0552
1.70 0.625
29LA.3.1 0.26
667
161
0.25
46.0
496.8 ±8,1
497.9 ±8,3
497.6 ±8,5
421
±37
−15
12.45 1.70
0.0573 0.99
12.48
1.70
0.0552
1.60
0.61
2.40
0.0801
1.70 0.719
29LA.4.1 0.23
914
228
0.26
44.2
352.0 ±5,8
352.9 ±5,9
352.9 ±6,1
265
±32
−25
17.78 1.70
0.0534 1.10
17.82
1.70
0.0515
1.40
0.40
2.20
0.0561
1.70 0.775
29LA.5.1 0.92
109
45
0.43
13.2
843.0
±17
847.0
±18
851.0 ±18
721
±66
−14
7.09
2.10
0.0711 1.50
7.15
2.10
0.0634
3.10
1.22
3.80
0.1397
2.10 0.570
29LA.6.1 0.14 1500 792
0.55
96.5
464.7 ±7,5
465.3 ±7,6
466.6 ±8,2
423
±18
−9
13.36 1.70
0.0565 0.60
13.38
1.70
0.0553
0.81
0.57
1.90
0.0747
1.70 0.899
29LA.7.1 0.47
220
112
0.52
18.4
595.1 ± 9,9
597.0
±10
599.0
±11
513
±48
−14
10.29 1.70
0.0614 1.30
10.34
1.70
0.0576
2.20
0.77
2.80
0.0967
1.70 0.624
29LA.8.1 1.07
156
90
0.60
13.3
607.0
±10
611.0
±11
613.0
±11
410
±84
−32
10.02 1.80
0.0638 1.50
10.13
1.80
0.0549
3.80
0.75
4.20
0.0987
1.80 0.427
29LA.9.1 0.10
346
121
0.36
21.7
453.0 ±7,6
452.6 ±7,7
454.3 ±8,1
481
±43
6
13.72 1.70
0.0576 1.60
13.74
1.70
0.0567
2.00
0.57
2.60
0.0728
1.70 0.665
29LA.10.1 0.21
866
374
0.45
67.7
560.3
±9
560.4 ±9,2
559.5 ±9,7
556
±22
−1
10.99 1.70
0.0604 0.82
11.01
1.70
0.0587
1.00
0.74
2.00
0.0908
1.70 0.856
29LA.11.1 0.15
746
366
0.51
56.6
544.7 ±8,8
545.0
±9
544.6 ±9,5
531
±24
−2
11.32 1.70
0.0593 0.91
11.34
1.70
0.0580
1.10
0.71
2.00
0.0882
1.70 0.839
29LA.12.1 0.84
80
58
0.75
6.5
577.0
±11
581.0
±11
576.0 ±12
397
±120
−31
10.58 1.90
0.0615 2.60
10.67
1.90
0.0546
5.10
0.71
5.50
0.0937
1.90 0.353
29LA.13.1 0.09
862
545
0.65
73.2
607.0
±10
607.0
±10
607.0
±11
622
±20
3
10.12 1.70
0.0612 0.79
10.13
1.70
0.0605
0.91
0.82
2.00
0.0987
1.70 0.887
29LA.14.1 0.28
173
175
1.04
52.1
1 928.0 ±29
1 904.0 ±33
1 925.0 ±34
2 095
±13
9
2.86
1.80
0.1322 0.66
2.87
1.80
0.1298
0.76
6.24
1.90
0.3486
1.80 0.917
29LA.15.1 0.31
334
104
0.32
42.0
878.0
±14
878.0
±15
879.0 ±15
891
±33
1
6.83
1.70
0.0713 0.99
6.85
1.70
0.0687
1.60
1.38
2.40
0.1460
1.70 0.729
29LA.16.1 1.14
60
17
0.29
10.8
1 203.0 ±21
1 201.0 ±22
1 210.0 ±22
1 269
±71
5
4.81
1.90
0.0926 2.30
4.87
1.90
0.0830
3.60
2.35
4.10
0.2052
1.90 0.469
29LA.16.2 0.19 1286
28
0.02
84.7
475.2 ±7,9
475.7
±8
475.8 ±7,9
441
±21
−7
13.05 1.70
0.0572 0.76
13.07
1.70
0.0557
0.94
0.59
2.00
0.0765
1.70 0.878
29LA.17.1 0.61
45
45
1.04
3.9
622.0
±14
622.0
±14
633.0 ±17
600
±130
−3
9.82
2.30
0.0649 3.30
9.88
2.30
0.0599
6.00
0.84
6.40
0.1012
2.30 0.357
29LA.18.1 0.19
870
313
0.37
45.8
383.0
6.30
383.7 ±6,4
383.9 ±6,7
316
±34
−17
16.31 1.70
0.0543 1.00
16.34
1.70
0.0527
1.50
0.45
2.30
0.0612
1.70 0.745
29LA.18.2 0.78
167
48
0.29
8.4
365.0
6.60
366.6 ±6,6
364.6
±7
206
±120
−44
17.03 1.80
0.0566 2.50
17.17
1.90
0.0502
5.10
0.40
5.40
0.0583
1.90 0.342
29LA.19.1 0.07
234
139
0.62
74.3
2 030.0 ±30
2 002.0 ±34
2 032.0 ±32
2 195
±10
8
2.70
1.70
0.1380 0.55
2.70
1.70
0.1374
0.58
7.01
1.80
0.3702
1.70 0.948
29LA.20.1 0.03 1065 861
0.84
87.5
588.7 ±9,4
588.4 ±9,6
590.0
±11
606
±17
3
10.45 1.70
0.0603 0.71
10.46
1.70
0.0601
0.80
0.79
1.90
0.0956
1.70 0.903
29LA.21.1 0.11
843 1686
2.07
67.2
571.4 ±9,2
571.8 ±9,4
580.0 ±14
549
±23
−4
10.78 1.70
0.0594 0.83
10.79
1.70
0.0585
1.10
0.75
2.00
0.0927
1.70 0.847
29LA.22.1 0.56
272
187
0.71
22.4
586.0
±10
588.0
±11
591.0 ±12
472
±55
−19
10.45 1.90
0.0611 1.40
10.51
1.90
0.0565
2.50
0.74
3.10
0.0951
1.90 0.600
29LA.23.1 0.50
210
81
0.40
21.5
724.0
±13
725.0
±13
710.0 ±14
676
±47
−7
8.37
1.90
0.0662 1.40
8.42
1.90
0.0621
2.20
1.02
2.90
0.1188
1.90 0.648
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
(1) Common Pb corrected using measured
204
Pb.
(2) Common Pb corrected by assuming
206
Pb/
238
U–
207
Pb/
235
U age-concordance
(3) Common Pb corrected by assuming
206
Pb/
238
U–
208
Pb/
232
Th age-concordance
vii
ZIRCON GEOCHRONOLOGY FROM CARBONIFEROUS–PERMIAN SANDSTONES (WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Table S2 (continued): New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken
from Vozárová et al. 2013, are shaded.
Hámor Fm.
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th/
238
U
ppm
206
Pb*
(1)
206
Pb/
238
U
Age
±1s
err
(1)
207
Pb/
206
Pb
Age
±1s
err
%
Discordant
(1)
238
U/
206
Pb
*
±%
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
/
235
U
±%
(1)
206
Pb
*
/
238
U
±%
err
corr
GZ-27.1.1
1.00
96
113
1.22
7.0
522
9
667
207
28
11.85
1.8
0.0618
9.7
0.72
9.8
0.0844
1.8
0.180
GZ-27.2.1
0.20
74
125
1.74
24.4
2077
20
2107
29
1
2.63
1.1
0.1307
1.7
6.85
2.0
0.3801
1.1
0.558
GZ-27.3.1
-0.11
137
133
1.00
58.7
2608
22
2832
26
9
2.01
1.0
0.2007
1.6
13.80
1.9
0.4987
1.0
0.550
GZ-27.4.1
0.06
112
96
0.88
54.4
2886
23
2936
13
2
1.77
1.0
0.2140
0.8
16.66
1.3
0.5647
1.0
0.770
GZ-27.5.1
-0.01
228
57
0.26
80.9
2232
15
2396
32
7
2.42
0.8
0.1544
1.9
8.81
2.1
0.4138
0.8
0.392
GZ-27.6.1
0.27
49
38
0.82
16.1
2101
24
2066
38
−2
2.59
1.4
0.1276
2.2
6.78
2.6
0.3854
1.4
0.532
GZ-27.7.1
0.03
437
126
0.30
172.2
2435
14
2552
15
5
2.18
0.7
0.1694
0.9
10.72
1.1
0.4589
0.7
0.609
GZ-27.8.1
0.03
1318
191
0.15
494.1
2334
12
2451
6
5
2.29
0.6
0.1596
0.4
9.60
0.7
0.4363
0.6
0.869
GZ-27.9.1
0.09
1501
408
0.28
63.4
309
2
278
46
−10
20.36
0.7
0.0518
2.0
0.35
2.1
0.0491
0.7
0.343
GZ-27.10.1
0.00
542
285
0.54
237.3
2654
14
2681
15
1
1.96
0.7
0.1831
0.9
12.86
1.1
0.5094
0.7
0.589
GZ-27.11.1
0.15
428
252
0.61
29.5
497
4
433
52
−13
12.47
0.8
0.0555
2.3
0.61
2.4
0.0802
0.8
0.319
GZ-27.12.1
0.15
126
104
0.85
10.2
577
6
587
78
2
10.68
1.1
0.0595
3.6
0.77
3.8
0.0936
1.1
0.296
GZ-27.13.1
0.02
1146
943
0.85
48.2
308
2
236
34
−23
20.44
0.7
0.0509
1.5
0.34
1.6
0.0489
0.7
0.410
GZ-27.14.1
0.07
101
45
0.46
45.0
2689
21
2709
15
1
1.93
1.0
0.1862
0.9
13.29
1.3
0.5177
1.0
0.718
GZ-27.15.1
0.32
134
215
1.66
8.5
460
5
476
124
3
13.50
1.2
0.0566
5.6
0.58
5.7
0.0740
1.2
0.204
GZ-27.16.1
0.09
605
538
0.92
42.3
504
3
467
35
−7
12.30
0.7
0.0564
1.6
0.63
1.7
0.0813
0.7
0.394
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
Error in Standard calibration was 0.4 % (not included in above errors but required when comparing data from different mounts).
(1) Common Pb corrected using measured
204
Pb.
viii
VOZÁROVÁ, ŠARINOVÁ, LAURINC, LEPEKHINA, VOZÁR, RODIONOV and LVOV
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Table S2 (continued): New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken from Vozárová
et al. 2013, are shaded.
Petrova Hora Fm.
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th/
238
U ppm
206
Pb*
(1)
206
Pb/
238
U
Age
(2)
206
Pb/
238
U
Age
(1)
207
Pb/
206
Pb
Age
%
Discordant
Total
238
U/
206
Pb ±%
Total
207
Pb/
206
Pb ±%
(1)
238
U
206
Pb
*
±%
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
*
/
235
U ±%
(1)
206
Pb
*
/
238
U ±%
err
corr
74LA_1.1
0.00
139
67
0.49
50.6
2270.0
±45
2280.0
±55
2222
±12
−2
2.37
2.30
0.1396
0.71
2.37
2.3
0.1396
0.71
8.12
2.40
0.4220
2.30 0.956
74LA_2.1
0.06
708
65
0.09
43.9
448.9
±8,4
449.0
±8,5
437
±23
−3
13.86
1.90
0.0561
0.93
13.87
1.9
0.0556
1.00
0.55
2.20
0.0721
1.90 0.885
74LA_3.1
0.09
646
379
0.61
32.7
368.1
±6,9
368.1
±7
365
±31
−1
17.00
1.90
0.0546
1.10
17.02
1.9
0.0539
1.40
0.44
2.40
0.0588
1.90 0.818
74LA_4.1
0.00
421
163
0.40
54.3
901.0
±16
902.0
±17
885
±16
−2
6.67
1.90
0.0685
0.77
6.67
1.9
0.0685
0.77
1.42
2.10
0.1500
1.90 0.929
74LA_5.1
0.12
2422
858
0.37
116.0
350.3
±6,5
350.5
±6,6
327
±23
−7
17.89
1.90
0.0540
0.90
17.91
1.9
0.0530
1.00
0.41
2.20
0.0558
1.90 0.881
74LA_6.1
0.24
500
68
0.14
24.2
352.5
±6,7
352.5
±6,8
356
±43
1
17.75
1.90
0.0556
1.40
17.79
2.0
0.0536
1.90
0.42
2.70
0.0562
2.00 0.713
74LA_7.1
0.05
214
99
0.48
14.6
493.1
±9,4
493.2
±9,6
489
±37
−1
12.57
2.00
0.0573
1.60
12.58
2.0
0.0569
1.70
0.62
2.60
0.0795
2.00 0.766
74LA_8.1
0.51
15
6
0.42
2.6
1201.0
±31
1200.0
±33
1215
±140
1
4.86
2.80
0.0850
5.70
4.88
2.8
0.0807
7.00
2.28
7.60
0.2048
2.80 0.376
74LA_9.1
0.58
129
1
0.01
7.8
433.2
±8,6
433.5
±8,7
408
±83
−6
14.30
2.00
0.0596
2.10
14.39
2.0
0.0549
3.70
0.53
4.20
0.0695
2.00 0.486
74LA_10.1 0.07
427
143
0.34
17.4
298.4
±5,7
298.4
±5,8
291
±45
−2
21.09
2.00
0.0527
1.70
21.11
2.0
0.0521
2.00
0.34
2.80
0.0474
2.00 0.708
74LA_11.1 0.12
611
389
0.66
39.2
464.0
±8,7
464.2
±8,8
452
±29
−3
13.38
1.90
0.0570
1.10
13.40
1.9
0.0560
1.30
0.58
2.30
0.0746
1.90 0.824
74LA_12.1 0.21
125
63
0.52
7.9
455.8
±9,1
455.8
±9,3
459
±65
1
13.62
2.10
0.0578
2.50
13.65
2.1
0.0562
2.90
0.57
3.60
0.0733
2.10 0.578
74LA_13.1 0.11
512
147
0.30
21.2
303.4
±5,8
303.4
±5,9
301
±40
−1
20.73
2.00
0.0533
1.60
20.75
2.0
0.0524
1.80
0.35
2.60
0.0482
2.00 0.744
74LA_14.1 0.02
587
228
0.40
35.1
433.9
±8,2
434.2
±8,3
408
±28
−6
14.36
1.90
0.0551
1.20
14.36
1.9
0.0549
1.20
0.53
2.30
0.0696
1.90 0.845
74LA_15.1 0.37
116
121
1.08
15.4
923.0
±17
924.0
±18
910
±44
−1
6.47
2.00
0.0725
1.60
6.49
2.0
0.0694
2.20
1.47
3.00
0.1540
2.00 0.686
74LA_16.1 0.11
653
433
0.69
31.0
346.4
±6,6
346.5
±6,6
345
±32
0
18.09
1.90
0.0543
1.30
18.11
1.9
0.0534
1.40
0.41
2.40
0.0552
1.90 0.808
74LA_17.1 0.09
597
172
0.30
31.1
379.4
±7,2
379.4
±7,2
382
±38
1
16.48
1.90
0.0550
1.50
16.49
1.9
0.0543
1.70
0.45
2.60
0.0606
1.90 0.751
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
Error in Standard calibration was 0.5 % (not included in above errors but required when comparing data from different mounts).
(1) Common Pb corrected using measured
204
Pb.
(2) Common Pb corrected by assuming
206
Pb/
238
U–
207
Pb/
235
U age-concordance
ix
ZIRCON GEOCHRONOLOGY FROM CARBONIFEROUS–PERMIAN SANDSTONES (WESTERN CARPATHIANS)
GEOLOGICA CARPATHICA
, 2019, 70, 6, 512–530
Table S2 (continued): New U–Pb (SHRIMP) detrital zircon age data from the Carboniferous–Permian sedimentary formations of the Northern Gemericum. Note: the old zircon age data from the sample LA-66, taken
from Vozárová et al. 2013, are shaded.
Novoveská Huta Fm. – new and older, recalculated, published data (gray)
Spot
%
206
Pb
c
ppm
U
ppm
Th
232
Th/
238
U
ppm
206
Pb*
(1)
206
Pb/
238
U
Age
(1)
207
Pb/
206
Pb
Age
%
Discordant
(1)
207
Pb
*
/
206
Pb
*
±%
(1)
207
Pb
*
/
235
U
±%
(1)
206
Pb
*
/
238
U
±%
err
corr
66LA_1.1
0.28
526
178
0.35
22.0
305.9
±6,1
251.0
±63
−18
0.0512
2.70
0.34
3.4
0.0486
2.0
0.595
66LA_2.1
0.04
798
186
0.24
32.8
301.1
±5,9
279.0
±40
−7
0.0518
1.80
0.34
2.7
0.0478
2.0
0.754
66LA_3.1
0.69
339
186
0.57
13.0
279.5
±5,8
128.0
±140
−54
0.0486
5.80
0.30
6.2
0.0443
2.1
0.340
66LA_4.1
0.11
348
173
0.51
13.3
280.6
±5,9
285.0
±77
2
0.0520
3.40
0.32
4.0
0.0445
2.2
0.540
66LA_5.1
0.74
174
17
0.10
8.7
361.1
±7,7
230.0
±140
−36
0.0508
5.90
0.40
6.3
0.0576
2.2
0.348
66LA_6.1
0.08
478
194
0.42
24.0
366.0
±7,4
320.0
±52
−13
0.0528
2.30
0.43
3.1
0.0584
2.1
0.670
66LA_7.1
0.09
1865
447
0.25
97.2
379.3
±7,4
394.0
±26
4
0.0546
1.20
0.46
2.3
0.0606
2.0
0.866
66LA_8.1
0.09
450
315
0.72
36.9
588.0
±12
541.0
±36
−8
0.0583
1.60
0.77
2.6
0.0955
2.0
0.784
66LA_9.1
0.00
646
295
0.47
26.5
301.1
±6,1
304.0
±41
1
0.0524
1.80
0.35
2.7
0.0478
2.1
0.750
66LA_10.1
−
610
136
0.23
312.0
3012.0
±49
2725.0
±15
−10
0.1881
0.91
15.44
2.2
0.5950
2.1
0.914
66LA_11.1
0.01
261
68
0.27
120.0
2760.0
±52
2697.3
± 9,9
−2
0.1849
0.60
13.62
2.4
0.5340
2.3
0.969
66LA_12.1
0.06
180
106
0.61
60.4
2130.0
±39
2314.0
±22
9
0.1472
1.30
7.95
2.5
0.3916
2.1
0.859
66LA_13.1
0.37
435
58
0.14
27.6
458.0
±9,2
457.0
±78
0
0.0561
3.50
0.57
4.1
0.0736
2.1
0.509
66LA_14.1
0.36
612
235
0.40
24.8
296.1
±6
160.0
±100
−46
0.0492
4.30
0.32
4.8
0.0470
2.1
0.431
66LA_15.1
0.21
461
135
0.30
19.0
301.9
±6,2
254.0
±92
−16
0.0513
4.00
0.34
4.5
0.0480
2.1
0.466
66LA_16.1
0.00
227
115
0.52
9.2
295.3
±6,3
240.0
±88
−19
0.0510
3.80
0.33
4.4
0.0469
2.2
0.496
66LA_17.1
0.06
554
343
0.64
28.1
369.8
±7,4
377.0
±57
2
0.0541
2.60
0.44
3.3
0.0590
2.1
0.630
66LA_17.2
−
835
225
0.28
42.8
374.3
±8,4
419.0
±50
12
0.0552
2.20
0.46
3.2
0.0598
2.3
0.718
66LA_18.1
−
217
235
1.12
10.8
363.7
±7,9
411.0
±69
13
0.0550
3.10
0.44
3.8
0.0580
2.2
0.587
66LA_19.1
0.18
616
237
0.40
31.1
367.3
±7,5
413.0
±56
13
0.0550
2.50
0.45
3.3
0.0586
2.1
0.638
66LA_20.1
0.23
614
45
0.08
40.1
471.3
±9,7
480.0
46.00
2
0.0567
2.10
0.59
3.0
0.0759
2.1
0.716
66LA_21.1
0.50
378
186
0.51
18.5
356.1
±7,8
382.0
±100
7
0.0543
4.60
0.43
5.2
0.0568
2.2
0.435
66LA_22.1
0.16
596
350
0.61
22.4
275.8
±5,9
227.0
±80
−18
0.0507
3.50
0.31
4.1
0.0437
2.2
0.536
66LA_24.1
0.06
1696
32
0.02
83.0
356.8
±6,7
346.0
±21
−3
0.0534
0.91
0.42
2.1
0.0569
1.9
0.903
66LA_25.1
0.25
121
72
0.62
38.6
2023.0
±35
2090.0
±15
3
0.1294
0.86
6.58
2.2
0.3686
2.0
0.921
66LA_26.1
0.03
806
561
0.72
38.9
352.7
±6,6
335.0
±28
−5
0.0532
1.20
0.41
2.3
0.0562
1.9
0.846
66LA_27.1
0.00
443
332
0.77
21.9
360.2
±6,9
333.0
±36
−7
0.0531
1.60
0.42
2.5
0.0575
2.0
0.778
66LA_28.1
0.12
424
9
0.02
28.3
480.8
±9
452.0
±36
−6
0.0560
1.60
0.60
2.5
0.0774
2.0
0.773
66LA_29.1
0.16
110
56
0.53
7.8
513.0
±10
474.0
±66
−7
0.0566
3.00
0.65
3.6
0.0828
2.1
0.572
66LA_30.1
0.27
400
80
0.21
27.5
495.3
±9,3
473.0
±42
−4
0.0565
1.90
0.62
2.7
0.0799
2.0
0.718
66LA_31.1
0.04
713
170
0.25
156.0
1462.0
±25
1502.2
±9,8
3
0.0937
0.52
3.29
2.0
0.2546
1.9
0.966
66LA_32.1
0.02
681
710
1.08
290.0
2598.0
±48
2653.2
±4,2
2
0.1800
0.25
12.32
2.3
0.4960
2.2
0.994
66LA_33.1
0.02
561
143
0.26
38.3
493.6
±9,2
485.0
±26
−2
0.0568
1.20
0.62
2.3
0.0796
1.9
0.854
Errors are 1-sigma; Pb
c
and Pb* indicate the common and radiogenic portions, respectively.
Error in Standard calibration was 0.64 %
(1) Common Pb corrected using measured
204
Pb.