GeolCarp_Vol68_No6_530

GEOLOGICA CARPATHICA

, DECEMBER 2017, 68, 6, 530–542

doi: 10.1515/geoca-2017-0035

www.geologicacarpathica.com

Late Permian volcanic dykes in the crystalline basement

of the Považský Inovec Mts. (Western Carpathians):

U–Th–Pb zircon SHRIMP and monazite chemical dating

ONDREJ PELECH

, ANNA VOZÁROVÁ

, PAVEL UHER

, IGOR PETRÍK

, DUŠAN PLAŠIENKA

KATARÍNA ŠARINOVÁ

and NIKOLAY RODIONOV

State Geological Institute of Dionýz Štúr, Mlynská dolina 1, 817 01 Bratislava, Slovakia; ondrej.pelech@geology.sk

Department of Mineralogy and Petrology, Natural Sciences Faculty, Comenius University in Bratislava, Mlynská dolina, Ilkovičova 6,

842 15 Bratislava, Slovakia

Earth Science Institute, Slovak Academy of Sciences, Dúbravská cesta 9, P.O. Box 106, 840 05 Bratislava, Slovakia

Department of Geology and Paleontology, Natural Sciences Faculty, Comenius University in Bratislava, Mlynská dolina, Ilkovičova 6,

842 15 Bratislava, Slovakia

All-Russian Geological Research Institute (VSEGEI), Sredny prospect 74, 199 106 St.- Petersburg, Russia

(Manuscript received November 29, 2016; accepted in revised form September 28, 2017)

Abstract: This paper presents geochronological data for the volcanic dykes located in the northern Považský Inovec Mts.

The dykes are up to 5 m thick and tens to hundreds of metres long. They comprise variously inclined and oriented lenses,

composed of strongly altered grey-green alkali basalts. Their age was variously interpreted and discussed in the past.

Dykes were emplaced into the Tatricum metamorphic rocks, mostly consisting of mica schists and gneisses of the

Variscan (early Carboniferous) age. Two different methods, zircon SHRIMP and monazite chemical dating, were applied

to determine the age of these dykes. U–Pb SHRIMP dating of magmatic zircons yielded the concordia age of

260.2 ± 1.4 Ma. The Th–U–Pb monazite dating of the same dyke gave the CHIME age of 259 ± 3Ma. Both ages confirm

the magmatic crystallization at the boundary of the latest Middle Permian to the Late Permian. Dyke emplacement was

coeval with development of the Late Paleozoic sedimentary basin known in the northern Považský Inovec Mts. and could

be correlated with other pre-Mesozoic Tethyan regions especially in the Southern Alps.

Key words: Permian volcanism, dykes, zircon dating, monazite dating, Western Carpathians, Tatricum.

Introduction

The occurrence of Upper Paleozoic sequences overlying the

Variscan crystalline basement is documented in various regions

of Europe from the Bohemian Massif to the Pyrenees (e.g.,

Wilson et al. 2004). A similar situation is also known in the

Western Carpathians, an Alpine thrust belt located in the eastern

continuation of the Eastern Alps. The Western Carpathians

represent north-vergent nappes that are traditionally divided

into Outer and Inner zones. The Inner Western Carpathians

consist of both thick- and thin-skinned Mesozoic nappes and

in the north are rimmed by the Cenozoic belt consisting of the

thin-skinned Outer Carpathians (Biely et al. 1996; Mišík 1997;

Plašienka et al. 1997; Lexa et al. 2000; Hók et al. 2014).

The northern part of the Inner Western Carpathians exposed in

the so-called Tatra–Fatra Belt (or simply the “Core moun-

tains”) comprises Cenozoic horsts of the Tatricum crystalline

basement and its autochthonous sedimentary cover overridden

by the Mesozoic Fatricum and Hronicum cover nappes.

The Tatricum, mostly consisting of Variscan crystalline base-

ment, is known for locally preserved Upper Paleozoic conti-

nental volcano-sedimentary sequences found in several of the

mountain ranges within the Tatra-Fatra Belt (Vozárová &

Vozár 1988; Vozár 1997; Ivan et al. 2002; Vozár et al. 2010).

However, only the region of the northern part of the Považský

Inovec Mountains is known for the presence of Carboniferous

terrigenous clastics and Permian volcanoclastic and volcanic

rocks (Putiš 1983; Štimmel et al. 1984; Olšavský 2008).

Occurrences of volcanic and/or sub-volcanic dykes in the

Western Carpathian Tatricum and Veporicum crystalline base-

ment are known from the Malé Karpaty Mts., Strážovské

vrchy Mts., Malá Fatra Mts., Nízke Tatry Mts. and Veporic

Kohút zone. They form a heterogeneous rock group usually

classified as the quartz porphyrites or lamprophyres (Hovorka

1967; Hovorka et al. 1982). Some of them are dated as Meso-

zoic (e.g., Spišiak & Balogh 2002) but the exact age of most of

them is still unknown.

The studied dykes occur in the crystalline basement of the

Selec (northern) Block of the Považský Inovec Mts. (Figs. 1, 2;

Ivanička et al. 2007, 2011). The pre-Alpine crystalline base-

ment of the Tatricum in the Selec Block is predominantly

composed of monotonous Variscan chlorite-muscovite (mica)

schists (dated as late Carboniferous, 307–310 Ma by Kráľ et

al. 2013), and only locally accompanied by quartz-rich para-

gneisses and amphibolites (cf. Krist et al. 1992). The basement

is covered by Upper Paleozoic to Jurassic and Upper Creta-

ceous complexes (Ivanička et al. 2007, 2011). The Upper

Paleozoic volcano-sedimentary Kálnica Group is known for

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, 2017, 68, 6, 530–542

Košice

Banská
Bystrica

Bratislava

17°

18°

19°

20°

21°

22°

49°

48°

S L O V A K I A

0 25 50 75 100

Považský Inovec Mts.
Fig. 2A

Fig. 2. A — Simplified tectonic map of the Považský Inovec Mts. with the studied area outlined.

Legend: 1 – Crystalline basement; 2 – Upper Paleozoic rocks of Tatricum; 3 – Triassic rocks of

Tatricum; 4 – Fatricum; 5 – Hronicum 6 – Upper Cretaceous rocks; 7 – Cenozoic sediments.

B — Geological map of the studied area in the northern Považský Inovec Mts. (modified after Elečko

et al. 2008). For the strati graphy of particular Upper Paleozoic formations see Fig. 3.

the occurrences of the Permian basalts and rhyolites (Fig. 3;

Vozárová & Vozár 1988; Rojkovič & Novotný 1993;

Korikovsky et al. 1995; Vozár 1997; Putiš et al. 2008; Olšavský

2008). The volcanic dykes scattered along numerous localities

in the crystalline basement of the northern Považský Inovec

Mts. were reported for the first time by Kamenický (1956) and

described in more detail by Polák (1956), who formerly

regarded them as products of Miocene volcanic activity. Dyke

rocks were classified as quartz porphyrites (dacites) and

referred to as post-Variscan, early Mesozoic in age (Hovorka

1960, 1967). In the following decades, several authors pro-

posed their age being Miocene (Hovorka & Spišiak 1988,

1990; Plašienka & Marko 1993). The more recent research

(Konečný 2005; Ivanička et al. 2011) brought more detailed

information about the spatial distribution of the dykes and

correlated them with quartz-bearing trachyandesites (TAQ),

which are unlikely to occur within the Miocene Central Slovak

Volcanic Field. This excluded a possibility of a Miocene age

and suggested an older (Cretaceous?) age. Remaining contro-

versy regarding the age of dykes and their relationship to

the other late Paleozoic or possibly Mesozoic volcanites in

the Považský Inovec Mts. (cf. Soták et al. 1993 and Putiš et al.

2008) as well other Permian volcanites in the Western

Carpathians (Vozár 1997) were the main reasons for our

attempt to date the dykes. These assumptions have been dis-

proved first by authors of this paper (Uher in Pelech 2015,

p. 59) who dated the dykes using monazite chemical dating as

approx. 259 Ma old. The same results were later obtained by

the monazite CHIME method by

other researchers (Putiš et al.

2016a) and U–Pb SIMS zircon

dating (Putiš et al. 2016b).

The main aim of this paper is to

present new geochronological

data obtained from the dykes in

the crystalline basement of the

northern (Selec) block of the

Považský Inovec Mts. by the means

of U–Th–Pb zircon SHRIMP and

monazite CHIME dating.

Regional geology

The studied dykes are intruded

into the crystalline basement rocks,

which are mostly composed of

chlorite-muscovite schists and

paragneisses (Fig. 4A and B),

only locally with amphibolite

lenses. Particularly the studied

locality is remarkable for contact

of dyke rocks with Permian ter-

rigenous sediments of the Tatri-

cum cover succession. The dykes

are 0.5 to 3m (locally up to 5m)

thick, lenticular bodies of grey-

green to grey-brown, volcanic

rocks with phenocrysts of quartz,

feldspars and mafic minerals.

Their length in map view varies

between tens of metres and

approx. 500 m. The orientation of

Fig. 1. Location of the Považský Inovec Mts. in the territory of

Slovakia.

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GEOLOGICA CARPATHICA

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Standard Chronostratigraphy

Period Epoch

Age/Stage

250

255

260

265

270

275

280

285

290

295

300

Carboniferous

Permian

Triassic

Cisuralian

Guadalupian

Lopingian

Early

Asselian

Sakmarian

Artinskian

Kungurian

Roadian

Wordian

Capitanian

Wuchiapingian

Changhsingian

Induan

Olenekian

258.8 +3.1

2.8 Ma

−

260.2 ± 1.4 Ma

Mnz

Dyke

age

305

Kasimovian

Gzhelian

Lat

Pennsylvanian

Moscovian

Middl

Pennsylvanian

310

Lúžna Fm.

Krivosúd Fm.

Novianska
Fm.

Selec
Fm.

Kálnica
Fm.

~ 280 Ma

(U/Th)

Lithostratigraphy

Dykes

quartz sandstone

grey-green volcano-
clastic sandstones
and conglomerates,
grey-green shales

violet and
grey arkose,
greywacke,
shales and
conglome-
rates

grey-green

arkose to

greywacke

metarhyolites

grey arkose with
white mica, breccias

metarhyolites

Putiš

et al. (2016b)

Rojkovi

Novotný

(19

)

mica schists,
with lenses of
gneisses and
amphibolites

riscan metamorphi

and deformatio

~310 ±3.5 Ma

Kráľ

et al

(2013)

dykes is variable, generally NW–SE to E–W. Intrusive con-

tacts are generally sharp (Fig. 4A and B), often marked by

chilled margins (Fig. 4C). Intrusion breccias along the dyke

walls containing clasts of the Upper Permian sandstones

(Krivosúd Formation) and underlying chlorite-muscovite

(mica) schists were observed at the Jablunkov vrch Hill loca-

lity (Fig. 4D). The occurrence of Permian sediments at the

dyke contact could be explained as a result of dyke propaga-

tion along the former normal or strike-slip faults. The dykes

contain up to 5cm thick quartz and hematite veinlets. Some

samples are lithologically similar to the Permian mafic volca-

nites occurring in the Hôrčanská dolina Valley in the western

part of the Považský Inovec Mts. (sample PI-1, Fig. 2B).

According to chemical composition, the dykes were characte-

rized as andesite to basaltic andesite (Hovorka 1960, 1967),

basaltic trachyandesite to trachyandesite (Konečný 2005) or

rhyodacite (Putiš et al. 2016b).

Several volcanic dykes were investigated in the Selec Block

of the Považský Inovec Mts. One rock sample PI-3 (approx.

10 kg weight) from the dyke at Jablunkov vrch Hill (elevation

794 m a. s. l.; GPS: N 48.7903°, E 18.0524°; Fig. 2), was col-

lected for U–Pb dating. Another sample PI-197B (approx. 1 kg)

from the same outcrop was used for the electron-microprobe

U–Th–Pb dating of monazite. Additionally, the sample PI-1

representing the Permian volcanites (Selec Formation, Figs. 2

and 3) from the Hôrčanská dolina Valley (GPS: N 48.70738°,

E 17.93374°) was used for petrographic and geochemical

correlation.

Analytical methods

Zircon crystals from the PI-3 sample were separated using

standard methods involving grinding, heavy liquid and mag-

netic separation procedures. The half-sectioned zircon crystals

were mounted in the epoxy resin puck with chips of the refe-

rence zircons TEMORA-1 (Black et al. 2003) and 91500

(Wiedenbeck et al. 1995). These were imaged by optical

microscopy, BSE and CL, in order to guide the positioning of

analytical spots. In situ U–Pb analyses were performed on

a SHRIMP-II at the Centre for Isotopic Research (CIR) at

VSEGEI in St. Petersburg, Russia. Each analysis consisted of

5 scans through the 196–254 AMU mass range; analytical pit

diameter was ~25 µm, with a primary O

−

beam intensity of

ca. 6 nA. The data have been reduced using the SQUID Excel

macro of Ludwig (2000). Common lead was corrected using

the measured

204

Pb/

206

Pb ratio and the Stacey & Kramers

(1975) model Pb evolution. Age calculations and plotting was

done with ISOPLOT/EX (Ludwig 2003). The uncertainties

given for individual analyses (ratios and ages) are at the one-

sigma level, but the uncertainties in calculated concordia ages

are reported at two-sigma levels.

The monazite age of the PI-197B sample were investigated

by electron microprobe in polished thin sections using

a Cameca SX100 electron microprobe (WDS mode) at the

Dionýz Štúr State Geological Institute, Bratislava. Further

details regarding the dating technique were published by

Konečný et al. (2004) and Petrík & Konečný (2009). A sample

current of 180 nA, counting times of 300 s for Pb, 80 s for

U and 35 s for Th and the accelerating voltage of 15 kV were

used. The beam diameter was typically 3–5 μm. For monazite

dating, we used ThMα

, UMβ

, PbMα

, YLα X-ray lines.

The interferences between PbMα

–YLγ

and UMα

–ThMβ

were corrected by empirically measured correction coeffi-

cients; interferences between REE X-ray lines were also cor-

rected, but these have no impact on the monazite dating

(Konečný et al. 2004). The statistical approach of Montel et al.

(1996) was applied for the final age determination and the

DAMON program was used for the age recalculations, histo-

grams and isochron plots (Konečný et al. 2004). Moreover, the

U/Pb vs. Th/Pb isochron method for monazite dating (CHIME;

Cocherie & Albarède 2001) was used.

The PI-3 and PI-1 samples were also analysed for major

and trace elements including REEs at the AcmeLabs Ltd.

Vancouver, Canada. Following a lithium metaborate/tetra borate

Fig. 3. Lithostratigraphy of the Upper Paleozoic Kálnica Group of the

northern Považský Inovec Mts. with marked occurrences of volcanic

rocks. R — Rhyolite; B — Basalt. The age of the investigated dyke as

indicated by zircon (Zr) and monazite (Mnz) dating (this paper) and

data by Putiš et al. (2016b).

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fusion and dilute nitric digestion, two instrumentation tech-

niques, inductively coupled plasma emission spectrometry

(ICP-ES) and inductively coupled plasma mass spectrometry

(ICP-MS), were used for whole-rock geochemical analyses.

Loss on ignition (LOI) represents weight difference deter-

mined separately after ignition at 1000 °C.

Results

Petrography

The dykes are composed of microporphyritic, grey-green

altered volcanic rocks (Fig. 4A–D). Textural evidence, espe-

cially the intersertal texture (Fig. 5A–B) points to a shallow

level of emplacement. The largest part of the PI-3 rock sample

consists of fine-grained aggregates of chlorite, Fe-oxide/

hydroxide minerals, calcite, albite, quartz and rare muscovite.

Fine needles of rutile and crystals of apatite are frequent. Laths

and needles of plagioclases are replaced by aggregates of

albite and muscovite. Mafic phenocrysts are totally replaced

by chlorite, Fe-oxides/hydroxide and quartz. Quartz crystals,

occurring in some thin-sections, show distinct magmatic cor-

rosion (Fig. 5C–F). Individual quartz crystals have embayed

margins and are wrapped by fine aggregates of chlorite and

opaque minerals (Fig. 5C–F). The majority of them are repre-

sented by volcanogenic β-quartz, but isolated polycrystalline

grains are also present (Fig. 5D). These partially dissolved

ß-quartz grains represent relicts of phenocrysts that were

incorpora ted into the ascending basalt dykes.

Mafic volcanites (sample PI-1), formerly mostly tuffs and

lava flows (Olšavský 2008), from the Selec Formation in the

Hôrčanská dolina Valley are represented by the dark green

unevenly foliated fine-grained rocks, where foliation oblite-

rated the initial rock texture. Microlites of plagioclases are

totally replaced by fine chlorite-sericite mixed layers and

albite. The interstices between feldspar microlites are occu-

pied by micro-crystalline aggregates of chlorite and Fe-Ti

oxides, associa ted with smaller amount of seri cite, albite and

quartz. Mafic pheno crysts are pseudomorphically repla ced by

Fe-Mg chlorite, Fe-Ti oxi des, and scarce calcite and quartz.

Magnetite and ilmenite were detected as primary magmatic

phase, either as inclusions in mafic phenocrysts or as indi-

vidual grains in the groundmass. Ilmenite was totally or par-

tially decomposed in rutile and hematite. According to the

preserved shape and system of cleavage, both rimmed or filled

by hematite, the observed phenocrysts correspond to amphi-

bole (Fig. 6). Rare square chlorite pseudomorphoses, occa-

sionally with inclusion of Cr-spinel, could have originated

after pyroxenes.

Fig. 4. A — Thinner dyke at the investigated locality Jablunkov vrch Hill. B — Thicker dyke at the northern slope of the Inovec Hill.

C — Brecciated contact of dyke and Permian sandstone at the investigated locality Jablunkov vrch Hill. D — Chilled margin of dyke on

the contact with the country rocks, marked by an arrow.

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(Winchester & Floyd 1977; Pearce 1996; Fig. 7). These immo-

bile elements classify the studied dyke as an alkali basalt

(sample PI-3) and volcanite to sub-alkaline basalt (sample

PI-1).

On the whole, both display chondrite-normalized rare earth

element (REE) patterns characterized by a slight enrichment

of light REEs (La

/ Yb

= 4.56 and 5.36, respectively) and

weak negative Eu-anomalies (Eu / Eu* = 0.80 and 0.91, respec-

tively), with no significant heavy REE fractionation (Fig. 5A;

Gd / Yb

= 1.55 and 1.58, respectively).

In the primitive mantle normalized multi-element diagram

(Fig. 5B) these rocks show a higher enrichment in Cs, Rb, Th,

U, Nb, K, Ta, LREE and Pb compared to Ba, Sr, P, Zr, Hf, Ti

and middle and heavy REE with distinct peaks for Cs, U, Th

and Pb and troughs for Ba, Nb, La-Ce, Sr and Ti. The studied

dyke rock (sample PI-3) has a low 0.51 Nb

/ Ta

ratio, similar

to 0.71 from the Selec Formation volcanite (sample PI-1).

These values are close to the 0.71 crustal ratio (Rudnick &

Fountain 1995), implying that crustal material has been assi-

milated. Equally, the crustal involvement is indicated by Nb/U

ratio (7.1 and 16, respectively) that confirms an assimilation

of crustal material (9.7 value for continental crust and 34

for mantle source according to Rudnick & Fountain 1995).

The primitive mantle normalized 0.18 (PI-3) and 0.67

(PI-1) Ce

/ Pb

ratios are consistent with the continental crust

(<1; Rudnick & Fountain 1995).

Zircon SHRIMP dating

Zircons mostly occur as short-prismatic crystals with

complicated oscillatory growth zoning. Zircon crystals ca.

200–400 μm long and 100–200 μm wide were used for

dating.

Intricate compositional growth zoning was identified within

the dated magmatic zircon grains by CL and BSE images

(Fig. 8A). Zircon crystals have a rather uniform internal

texture, characterized by a narrow fine oscillatory growth

zoning. In some zircon crystals, the regular growth zoning is

interrupted by textural discontinuities along which the original

zoning is resorbed or truncated and succeeded by new-growth

of zoned zircon rims (Fig. 8A, spots PI3-4, 6, 7). A very old

xenocrystic core (

207

Pb /

206

Pb 2101±17 Ma) was identified,

mantled by the newly grown magmatic zircon (Fig. 8A,

spot PI3-5).

The sample PI-3 yielded a cluster of

206

Pb /

238

U ages, ranging

between 258 Ma and 263 Ma, for nine magmatic zircon

Table 1: Major (wt. %) and trace-element (ppm) whole rock analyses of the Považský Inovec Mts. dated dyke sample PI-3 and volcanite PI-1

sample. Sum of iron (Fe

tot

) was measured as Fe

major oxide (wt. %)

Sample

SiO

MgO

CaO

TiO

MnO

LOI

sum

tot

PI-3

55.06

16.86

9.14

6.19

0.72

3.40

1.60

1.70

0.42

0.07

0.03

4.60

99.78

0.06

PI-1

48.5

14.3

9.61

4.18

8.09

3.36

1.13

1.85

0.34

0.16

0.02

8.60

99.82

1.76

trace element (ppm)

PI-3

111.0

118.0

34.8

2.5

18.5

4.1

27.7

93.0

69.8

3.1

2.9

3.9

142.0

174.6

30.0

PI-1

106

28.5

3.9

18.3

5.1

12.9

147.9

0.9

4.0

0.8

207

194.8

42.8

PI-3

22.10

43.30

5.6

22.60

5.19

1.60

5.48

0.93

5.35

1.8

2.96

0.45

2.80

0.41

9.80

PI-1

55.6

7.1

29.6

6.73

1.86

7.43

1.22

7.3

1.46

4.8

0.6

3.87

0.6

3.3

Fig. 6. BSE image of pseudomorph after mafic phenocryst of amphi-

bole, sample PI-1.

0.001

0.01

0.1

0.01

0.1

Nb/Y, ppm

Trachy-

andesite

Trachyte

Phono-

lite

Comendite

Pantellerite

Andesite/Basalt

Sub-alkaline basalt

Alkali basalt

Zr/T

, ppm

PI-3 - Dyke
PI-1 - Metavolcanite

PI-R11a, PI-R11b - Inter. volc.
PI-RD1 - Dyke

Data from Putiš et al. 2016b:

Rhyolite/dacite

Tephri-

phonolite

Foidite

Fig. 7. Zr/TiO

vs. Nb/Y diagram (Pearce 1996) showing classifica-

tion of dyke (PI-3) and volcanites (PI-1) from Považský Inovec Mts.

based on immobile elements. Circles represent data published by

Putiš et al. (2016b).

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crystals (Table 2; Figs. 8A and 9). The

232

Th/

238

U ratios are

mostly between 0.40 and 1.34, typical for zircons of a mag-

matic origin. U and Th contents are relatively low, 107–463

ppm and 69–427 ppm, respectively. The concordia age, calcu-

lated from the clusters along the concordia curve, is 260.2

±1.4 Ma (95 % confidence, decay-constant errors included;

MSWD = 0.63, probability = 0.43).

Monazite electronmicroprobe dating

Monazite is a very rare accessory mineral in the studied dyke

rocks. It forms euhedral to subhedral crystals, 20 to 50 μm

across, hosted by in K-feldspar and quartz phenocrysts

(Fig. 8B and C). Monazite associates with zircon, apatite and

rarely xenotime-(Y). Monazite crystals show regular oscilla-

tory zoning in BSE images. Locally, tiny inclusions of ThSiO

phase (thorite or huttonite) occur in monazite. Electron-

microprobe dating of monazite using the calculation method

of Montel et al. (1996) shows a weighted average age of

255 ± 4 Ma (26 point analyses, MSWD = 1.58). The histogram

of individual ages (Fig. 10A) shows an asymmetrical distribu-

tion slightly skewed to younger ages with the maximum age

intervals between 250–260 and 260–270 Ma. Deconvolution

of this histogram (Fig. 10B) gives 258.6 ± 4 Ma for the main

fraction (94 %, Isoplot 4.15) Standard Suzuki-type isochron

(Fig. 10 C) provides a good fit, but with the positive intercept

Fig. 8. A — Selected cathodoluminiscence magmatic zircon images from the Považský Inovec Mts. Permian dyke (sample PI-3) with indica-

tion of the age data (in Ma) based on

206

Pb/

238

U ratios. Zircon indicated by asterisk corresponds to the

207

Pb/

206

Pb age value of the Palaeoproterozoic

xenocrystic grain. B-C: BSE images of monazite-(Ce) from the studied volcanic rock, sample PI-197B. B — Crystal of monazite (white), partly

replaced by fluorapatite along the rims (grey) in chlorite-rich groundmass (dark grey). C — Regular oscillatory zoning of the same monazite

crystal.

Table 2: SHRIMP zircon age data from the sample PI-3. Errors are 1-sigma; Pbc 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.

(1)

Spot

206

232

Th/

238

206

Pb*

206

Pb/

238

U ±

207

Pb/

206

Pb ± Discor-

dant

206

Pb/

238

U ±

207

206

207

235

U ±

206

238

U ±

err

corr

ppm ppm

ppm

Age

PI3-1

0.16 178 100

0.58

6.36

262.7

2.1

262

24.4

0.83

0.0515

3.4

0.295

3.5

0.0416

0.83 .235

PI3-2

0.20 420 242

0.59

15.10

262.7

1.4

179

53 −32

24.4

0.56

0.0497

2.3

0.2848

2.3

0.0416

0.56 .240

PI3-3

0.21 330 427

1.34

11.60

258.4

1.8

233

64 −10

24.45

0.72

0.0508

2.8

0.2866

2.9

0.0409

0.72 .251

PI3-4

0.30 463 279

0.62

16.30

258.0

1.6

236

−8

24.48

0.62

0.0509

2.7

0.2866

2.8

0.0408

0.62 .225

PI3-5

0.20 107

0.50

32.60

1958

2101

2.816

0.73

0.1302

6.40

1.2

0.355

0.73 .592

PI3-6

0.60 134

0.53

4.73

258.5

2.9

117

140 −55

24.44

1.10

0.0484

5.7

0.2730

5.9

0.0409

1.10 .193

PI3-7

0.18 134

0.48

4.74

259.3

2.8

337

24.36

1.10

0.0532

3.9

0.3010

4.0

0.0410

1.10 .273

PI3-8

0.86 136

0.69

4.83

258.0

2.8

110

140 −57

24.49

1.10

0.0482

6.0

0.2710

6.1

0.0408

1.10 .183

PI3-9

0.30 268 114

0.44

9.46

259.0

2.0

289

24.40

0.80

0.0521

3.6

0.2940

3.7

0.0409

0.80 .215

PI3-10 0.00 189

0.40

6.79

263.4

2.4

327

23.97

0.92

0.0530

2.7

0.3046

2.9

0.0417

0.92 .320

537

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250

260

270

0.039

0.040

0.041

0.042

0.043

0.22

0.24

0.26

0.28

0.30

0.32

0.34

n = 9

Concordia Age = 260.2 ± 1.4 Ma

(2 , decay-const. errs included)

MSWD (of concordance) = 0.63

Probability (of concordance) = 0.43

data-point error ellipses are 2σ

207

235

Pb /

206

238

200

600

1000

1400

1800

2200

0.0

0.1

0.2

0.3

0.4

data-point error ellipses are 2σ

207

235

Pb /

206

238

Fig. 9. U/Pb concordia plot showing the magmatic zircon ages from the sample PI-3 dyke. A — all data; B — detail on concordia age data.

U/Pb

Th/Pb

100

data-point error ellipses are 2σ

Centroid age 258.8+3.1-2.8 Ma

Regression line

Isochron

U/Pb age 253.2+23.9-26.3

Th/Pb age 261.7+13.4-12.2

0.00

0.04

0.08

0.12

0.16

0.20

Th* (wt. %)

Pb (wt. %)

Age = 244 ± 22 Ma

MSWD=0.78

itcpt = 0.0050±0.0077

100

150

200

250

300

350

400

equency

Age (Ma)

258.6±4 Ma

230

220

240

250

260

270

280

290

Age 255 ± 3.4 Ma (2σ)

MSWD = 1.58

Number = 26

Age (Ma)

equency

Fig. 10. A — Histogram of apparent EMPA monazite-(Ce) ages (n = 26) from sample PI-197B. B — Deconvolution (by Isoplot 4.15) of

the histogram provides 94 % fraction of older age 258.6 ± 4 Ma, the younger age is neglected. C — Standard Suzuki-type CHIME weighed

isochron shows a positive intercept of 0.005 % Pb, which indicates an apparently younger age 244 ± 22 Ma. The shaded field is the 2SD error

envelope of the regression line. D — Th/Pb vs. U/Pb CHIME isochron (Cocherie & Albarede 2001, solid line) gives an almost concordant age

of 259 ± 3 Ma. The shaded field is the 2SD error envelope of the regression line.

538

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, 2017, 68, 6, 530–542

0.0050 ± 0.0077 indicating an apparently younger age which

is confirmed by the weighed isochron age of 244 ± 22 Ma

(Fig. 10B). Therefore, we prefer the U/Pb vs. Th/Pb isochron

calculation method (Cocherie & Albarède 2001), suitable

for monazite with variable U/Th ratios. In Fig. 10D, the spread

of data defines a concordant isochron giving the age

259 ± 3 Ma and low MSWD = 0.97 (Table 3). One measure-

ment point with an extremely high U content (3.8 wt. %)

was excluded. Contrary to the standard isochron, this age is

slightly higher than the weighted average and identical with

the deconvolution age (Fig. 10B), and it is considered the best

estimate.

Discussion

The age of volcanic dykes in the crystalline basement of the

northern (Selec) block of the Považský Inovec Mts. was

a matter of debate for a long time. Konečný (2005) compared

the studied rocks with Miocene volcanites from the Central

Slovak Volcanic Field. On the basis of petrographic and geo-

chemical criteria, he discussed several contradictory features

that excluded a Neogene age. The dykes from the Považský

Inovec Mts. compared with similar Neogene rocks of the

Central Slovak Volcanic Field, contain higher FeO tot

(10.55 – 7.17 wt. % vs 5.69 wt. %), MgO (8.93 – 4.02 wt. %

vs 2.39 wt. %), TiO (1.96 – 1.12 wt. % vs. 0.61) and P

(0.77 – 0.37 wt. % vs. 0.28) (data from Konečný 2005 and

present paper). A primary association of mafic minerals

(pyroxenes?, amphiboles), represented by the chlorite + quartz

+ Fe mineral pseudomorphoses (very rare with inclusion of

Cr-spinel; Konečný l.c.) was not found within the Neogene

dykes. Correspondingly, the hydrothermal alterations of the

compared rocks are different, chlorite + sericite + quartz ± calcite

in the Permian dykes versus biotite + K-feldspars + pyrite

+ sericite + argillite in the dykes of Neogene age. The zircon

U/Pb concordia age (260.2 ± 1.4 Ma; Fig. 9) as well as mona-

zite chemical dating (259 ± 3 Ma; Fig. 10) show latest a Middle

Permian (Capitanian) to Late Permian (Wuchiapingian, accor-

ding to Cohen et al. 2013 and ICS Chronostratigraphic chart

2017/2) crystallization age of the dyke in the Považský Inovec

Mts. The 2101 ± 17 Ma

207

Pb /

206

Pb age value (Table 2) indicates

a presence of xenocrystic Palaeoproterozoic zircon. It does not

represent a primary constituent of the magma since it was

assimilated from country rocks. The obtained late Permian age

is in accordance with ages obtained by U/Pb SIMS dating of

dykes and volcanites (Putiš et al. 2016 b). It is also supported

by the zircon fission track analysis of the crystalline basement

rocks which show late Permian post-Variscan cooling with

no signs of Alpine metamorphic overprint (Králiková et al.

2016).

According to the present results, the studied dykes are the

only dated representatives of late Paleozoic shallow volcanic

intrusions in the Tatricum found in situ until now. The petro-

logical and geochemical features differentiate the dykes from

similar dykes occurring in the Tatricum crystalline basement

which are mostly represented by lamprophyres (Hovorka

1967; Spišiak & Balogh 2002).

The volcanism of the Upper Paleozoic Kálnica Group is

believed to be bimodal and concentrated mainly in the Lower

Permian Selec Formation. The prevailing volcanic rocks are

represented by the basaltic tuffs and lava flows exposed

mainly in the Hôrčanská dolina and Hrádocká dolina Valleys.

These bodies are represented by volcanite sample PI-1 which

was correlated with the dated dyke (PI-3). Mafic volcanites

from the Kálnica Group are represented by subalkaline

within-plate type basalts (Korikovsky et al. 1995; Putiš et al.

2006). Less common rhyolites are known from the surface

only in the Hôrčanská dolina Valley where they represent part

of the Upper Permian Krivosúd Formation (Ivanička et al.

2007; Olšavský 2008). Other rhyolites were recorded in the

boreholes around the Klenkov vrch Hill and in the former

exploration galleries north of Selec village in the Lower

Permian Selec Formation (Štimmel et al. 1984; Olšavský

2008). Unfortunately, these occurrences are not accessible at

present. Rhyolites and their pyroclastic rocks of the Krivosúd

Formation from the Hôrčanská dolina Valley were recently

dated by Putiš et al. (2016b). They gained U–Pb zircon age

data in the range of 266.5 ± 1.9 Ma and 262.4 ± 2.1 Ma (Putiš

et al. l. c.) and confirmed the Upper Permian age of the

Krivosúd Formation proposed earlier (e.g., Štimmel et al.

1985; Olšavský 2008). Putiš et al. (2016 b) projected the

studied volcanites in the rhyolite field (in the sense of Le Bas

et al. 1986 and De La Roche et al. 1980 classifications). We

classified these rocks as rhyodacite/dacite and basalt/andesite

based on Zr /TiO

vs Nb / Y ratios (Pearce 1996; Fig. 7), for the

high mobility of alkalis. They are enriched in LREE and more

fractionated with the higher Eu anomalies in comparison with

basic rocks (Fig. 11A). Correspondingly, in the multi-element

diagram they are enriched in Th, La, Ce but depleted in Cs,

Rb, U, Nb, K, Pb, Sr and Ti (Fig. 11) compared with basic

volcanic rocks (sample PI-1; Fig. 11B).

The volcanic dyke that was formerly classified by Putiš

et al. (2016 b) as meta-rhyodacite (sample PI-RD 1) is geo-

chemically identical with our sample PI-3. Based on Zr/TiO

vs Nb/Y ratios (Pearce 1996) it corresponds to alkali basalts

(Fig. 7). Equally, distributions of REE and trace elements

show an absolutely equal tendency (Fig. 11A and B).

The obtained ages correspond to the Guadalupian–Lopingian

volcanic phase, possibly as a result of an extensional tectonic

regime, also documented in other Western Carpathian units,

as in the Northern Veporic (Vozárová et al. 2016), Hronic

Table 3: EMPA (U+Th) –Pb ages of monazite in the studied sample

PI-197B from the Považský Inovec Mts. Centroid age is the age

corresponding to the crossing of functions y = f(x) and x = f(y), where

x = U / Pb and y = Th / Pb.

Age Ma

2σ Ma

− 2σ Ma

Centroid age

258.8

3.1

2.8

Th/U age

261.7

13.4

12.2

U/Pb age

253.2

23.9

26.3

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DATING OF THE LATE PERMIAN VOLCANIC DYKES FROM THE POVAŽSKÝ INOVEC MTS.

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(andesite–basalts of the 2

eruption phase; Vozár 1997; Dostal

et al. 2003; Vozár et al. 2015) dated after the Illawara Reversal

Magnetic Horizon (Vozárová & Túnyi 2003), as well as from

the Bôrka Nappe (Vozárová et al. 2012) and Silicicum (Demko

& Hraško 2013).

As was noted by Ivan et al. (2002), the Permian volcanism

in the Western Carpathian region is analogous to the Ligurian

and Southern Alps and Sardinia (Cortesongo et al. 1998;

Dallagiovanna et al. 2009). However, Middle to Early Permian

volcanites are not known in adjacent regions containing

post-Variscan sedimentary basins, such as the Bohemian

Massif (Ulrych et al. 2006), Eastern Alps (Krainer et al. 2005)

or Eastern Carpathians (Seghedi et al. 2001).

The Považský Inovec Mts. dykes are located east of the

main occurrence of the Upper Paleozoic rocks (Fig. 2). Older

investigations described the dykes as NNE–SSW to NE–SW

trending and unaffected by the Alpine metamorphic overprint

(Maheľ 1986; Ivanička et al. 2011). This variation suggests the

possibility of different ages of variously oriented dykes (cf.

Shrivastava 2011) and will require further verification.

The oldest Upper Paleozoic sediments in the Tatricum are

represented by 100–250 m thick grey-green and black white-

mica bearing sandstones, black shales and conglomerates of

the Novianska Formation found only in the Považský Inovec

Mts. (Figs. 2B and 3). Its stratigraphic age was determined in

the Novianska dolina Valley as Carboniferous based on the

occurrence of microflora (Čorná & Kamenický 1976). The

Novianska Fm. overlies Variscan chlorite-muscovite schists,

dated by

Ar/

Ar method around 310–302 Ma old, and so to

the latest Carboniferous (Late Pennsylvanian, Kráľ et al.

2013). Additionally, the occurrence of clasts of the underlying

basement rocks found in the conglomerates of the Novianska

Fm. (Kamenický 1956; Putiš 1983; Olšavský 2008) indicates

that their sedimentation took place directly after the meta-

morphic event in the latest Carboniferous. This was a period

of rifting characterized by formation of restricted, probably

elongated, extensional basins as a result of post-collisional

collapse of the Variscan orogen. The later subsidence, charac-

terized by the deposition of continental sediments of the Selec

Fm. above the older Novianska Fm. or directly on the Variscan

crystalline basement rocks was accompanied by bimodal

subalkaline to alkaline volcanism in early Permian times

(Broska et al. 1993). The rhyolitic volcanism of this stage in

the Považský Inovec Mts. was accompanied by U-mine-

ralization, the syngenetic stage of which was dated to approx.

280–270 Ma (Rojkovič & Novotný 1993; Rojkovič 1997).

The latest Permian was characterized by subsidence affecting

larger parts of the Tatric–Veporic region. In the Tatricum

terrestrial clastics, usually with volcanic admixture are known

(the Devín, Krivosúd, Stráňany, Vážna and Meďodoly

Formations, cf. Vozárová & Vozár 1988; Vozárová 1996). Our

data indicate that the dykes were emplaced during this period

(∼260 Ma), most probably along faults. The studied dykes

(together with rhyolites dated by Putiš et al. 2016 b) are there-

fore the first representatives of the Upper Paleozoic volcanites

in the Tatricum to be dated by the means of modern geochro-

nological methods. The answer to the question whether they

served as magma feeders is not entirely clear. At present, there

is no documented occurrence of coeval (and comagmatic)

extrusive mafic rocks in the studied region. The originally

assumed uniform age of the dykes and basaltic volcanites

from the Selec Formation is also unlikely. The volcanogenic

admixture described in the late Permian Krivosúd Formation

is only felsic in character (Putiš 1983; Štimmel et al. 1984;

Olšavský 2008).

ß-quartz phenocrysts occurrence in the dyke rock in the

sample PI-3 (Fig. 5C and E) remains unusual and causes

problems for the petrographic classification of rocks (cf.

Putiš et al. 2016 b). Conditions for incorporation of quartz

crystals can occur, when the basaltic melts enter the residual

rhyolite magma chamber. The evidence of the interaction of

mafic magma with crustal material and quartz dissolution

were experimentally documented by Watson (1982) and

Donaldson (1985). However, the occurrence of quartz in

rocks of basaltic character could also be interpreted as a result

of contamination by country rocks (cf. Hovorka 1967) as it

is shown by the frequent presence of polycrystalline quartz

(Fig. 5 D).

100

1000

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Yb Lu

PI-1

PI-3

100

1000

PI-1

PI-3

Fig. 11. A — Chondrite-normalized REE patterns of the Považský Inovec Mts. Permian volcanic rock (PI-1) and dyke (PI-3). Normalizing

values are after McDonough & Sun (1995). B — Multi-elements variation diagram of the Považský Inovec Mts. Permian mafic volcanic rock

(PI-1) and dyke (PI-3). Normalizing values are after Sun & McDonough (1989).

540

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GEOLOGICA CARPATHICA

, 2017, 68, 6, 530–542

Conclusions

A volcanic dyke of alkali basalt composition (Figs. 4, 5

and 7) from the crystalline basement of the northern Považský

Inovec Mts. (Western Slovakia) was dated by the U–Pb zircon

SHRIMP and monazite U–Th–Pb EMPA methods. Both U–Pb

zircon SHRIMP (260.2 ±1.4 Ma) and monazite U–Th–Pb

EMPA dating (259 ±3 Ma) provided (within error) latest

Middle Permian to Late Permian (Capitanian/Wuchiapingian)

ages for the studied rocks. The dykes, together with volcanites

dated by Putiš et al. (2016 b) in the northern Považský Inovec

Mts., represent rare post-Variscan late Paleozoic volcanites,

the only ones known from the Tatricum up to now. The

obtained ages correspond to the Guadalupian–Lopingian

extensional tectonic regime also documented in the Hronicum,

Silicicum and Bôrka Nappe.

Acknowledgements: This work was supported by the Slovak

Research and Development Agency under the contracts

No. APVV-0546-11, APVV-14-0278, APVV-15-0050, APVV-

0212-12, VEGA Agency No. 1/0257/13 and 1/0499/16.

The first author is grateful for the fruitful discussions to P. Ivan

and Š. Méres during initial study of the topic and J. Hók for the

initial impulse to date the dykes. The manuscript benefitted

from discussions with R. Demko and the constructive com-

ments and remarks of two anonymous reviewers.

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