GeolCarp_Vol70_No4_298

GEOLOGICA CARPATHICA

, AUGUST 2019, 70, 4, 298–310

doi: 10.2478/geoca-2019-0017

www.geologicacarpathica.com

Recycling of Paleoproterozoic and Neoproterozoic crust

recorded in Lower Paleozoic metasandstones of

the Northern Gemericum (Western Carpathians,

Slovakia): Evidence from detrital zircons

ANNA VOZÁROVÁ



, NICKOLAY RODIONOV

and KATARÍNA ŠARINOVÁ

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

Centre of Isotopic Research, A.P. Karpinsky Russian Geological Research Institute (FGBU «VSEGEI»), Sredny prospekt 74,

199 106 St.-Petersburg, Russia

(Manuscript received February 20, 2019; accepted in revised form June 10, 2019)

Abstract: U–Pb (SHRIMP) detrital zircon ages from the Early Paleozoic meta-sedimentary rocks of the Northern

Gemericum Unit (the Smrečinka Formation) were used to characterize their provenance. The aim was to compare and

reconcile new analyses with previously published data. The detrital zircon age spectrum demonstrates two prominent

populations, the first, Late Neoproterozoic (545–640 Ma) and the second, Paleoproterozoic (1.8–2.1 Ga), with a minor

Archean population (2.5–3.4 Ga). The documented zircon ages reflect derivation of the studied metasedimentary rocks

from the Cadomian arc, which was located along the West African Craton. The acquired data supports close relations of

the Northern Gemericum basement with the Armorican terranes during Neoproterozoic and Ordovician times and also

a close palinspastic relation with the other crystalline basements of the Central Western Carpathians. In comparison,

the detrital zircons from the Southern Gemericum basement and its Permian envelope indicate derivation from

the Pan-African Belt–Saharan Metacraton provenance.

Keywords: SHRIMP dating, detrital zircon ages, provenance, palinspastic constraints.

Introduction

Detrital zircon age dating is a powerful tool in deciphering the

sedimentary provenance and tectonic evolution of continental

realms, and constraining the paleogeography (e.g., Gehrels et

al. 1995, 2000; McLennan et al. 2001; Stewart et al. 2001;

Dickinson & Gehrels 2003, 2008; Hervé et al. 2003; Allen et

al. 2006; Kolodner et al. 2006; Mueller et al. 2007; Lorenz et

al 2008; Balintoni et al. 2010; Drost et al. 2011; Ustaömer et

al. 2011; Zajzon et al. 2011; Avigad et al. 2012). In general,

the study of clastic sediments is crucial for paleotectonic

reconstructions as they can provide information about poten-

tial lithologies in ancient source areas. Particularly, the study

of detrital zircons is important in terranes with the occurrence

of siliciclastic sediments or metasedimentary rocks, lacking

any bio-stratigraphic evidence of their age. Furthermore, in

the absence of fossils and other stratigraphic data, the youn-

gest zircon grains in a sedimentary rock can indicate the maxi-

mum depositional age (e.g., Fedo et al., 2003; Meinhold &

Frei, 2008; Spencer et al. 2016).

In this paper, detrital zircon U–Pb ages for the Smrečinka

metasandstones are presented, which belong to the basal part

of the Rakovec Group and, which have been assigned to

the pre-Carboniferous basement complexes of the Northern

Gemeric Unit (NGU) (Fig. 1). From a tectonic point of view,

the NGU represents the relic of the Variscan collision suture,

consisting of two distinct crystalline complexes and the rem-

nants of the Mississippian syn-orogenic basin-fill. Under-

standing the age and origin of the Smrečinka sedimentary

sequence may give innovative approaches to test a current

plate tectonic model, with implications for understanding

the evolution of the Northern Gemericum basement during

Paleozoic times.

The new zircon ages are interpreted in conjunctions with

one previously published sample from Vozárová et al. (2013).

We were able to put together a set of 93 analyses that provided

a more solid set of data than the previously published 44 ana-

lyses. In both studies an equally sensitive high-resolution ion

microprobe (SHRIMP) was applied to determine (Williams

1998; Larionov et al. 2004) the U–Pb ages of detrital zircon

grains. The U–Pb detrital zircon ages reported here have sig-

nificant implications that may inspire further work and discus-

sion of the role of the NGU zone during the Variscan orogeny

and for the structure of the Western Carpathians.

Geological background

In the sense of the latest syntheses on the geological struc-

ture of the Western Carpathians (Plašienka in Froitzheim et al.

2008; Plašienka 2018), the triple regional tectonic zonation is

generally accepted. This division includes the Inner Western

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, 2019, 70, 4, 298–310

Carpathians (IWC) in the south, the Central Western

Carpathians (CWC) in the middle, and Outer Western

Carpathians in the north. Each of these three major regional

zones include their own principal tectonic units, which were

incorporated into the growing orogenic wedge in particular

time periods, spanning in time from late Jurassic/early

Cretaceous to early Miocene, generally progressing from

south toward north (Plašienka 2018 and references therein).

Fragments of the Variscan crust with their post-Variscan

sedimentary cover were incorporated into the early and middle

Cretaceous tectonic units of the Central and Inner Western

Carpathians orogenic system.

The Northern Gemeric Unit (NGU) belongs to the inner-

most part of the CWC, and, as a whole, clearly overrides

the Veporicum along the Early Alpine thrust contact recog-

nized as the Lubeník–Margecany Line (LML; Andrusov

1959). Similarly, the tectonic contact of the NGU with the

adjacent Southern Gemeric Unit (SGU), which belongs to

the IWC zone, is represented by the Hrádok–Železník Line

(HZL) (defined by Abonyi 1971), that continues into a system

of thrust faults to the east (Fig. 1). The NGU is generally cor-

related with the Upper Austroalpine units, such as the eastern

Greywacke Zone in the Eastern Alps (Andrusov 1968; Maheľ

1986; Neubauer & von Raumer 1993; Schmid et al 2008, and

references therein).

The NGU contains relics of the Variscan collision suture,

from which thrust wedges of two pre-Carboniferous com-

plexes, the high-grade gneissic-amphibolites of the Klátov

complex and the low-grade Rakovec complex, are preserved

as well as relics of a Mississippian syn-orogenic turbidite

sequence (Vozárová & Vozár 1996). Each of these units is

lithologically distinct (Bajaník et al. 1983; Spišiak et al. 1985;

Hovorka et al. 1988; Vozárová & Vozár 1988; Ivan 1994, 1997,

and references therein). The mutual contact of both pre-Car-

boniferous crystalline basement complexes is tectonic, fol-

lowed by lenses of antigoritic serpentinites at the base of

the thrust plane. Deformational and metamorphic events recor-

ded by both pre-Carboniferous terranes occurred in the Late

Devonian/Mississippian but experienced later Alpine rewor-

king (Dallmayer et al. 1996, 2005; Vozárová et al. 2005; Putiš

et al. 2009). The Late Devonian/Mississippian deformation

and metamorphism are documented by reworked rock frag-

ments from both NGU crystalline complexes within the over-

stepping Pennsylvanian conglomerates (Vozárová 1973).

These events were also proved by geochronological data:

(i) 372 ± 3 Ma by Ar/Ar ages of muscovite from orthogneiss

pebble and 386 ± 3 Ma of detrital white mica from the over-

lying Pennsylvanian sandstones (Vozárová et al. 2005);

(ii) 386–372 Ma U–Pb ages from metamorphic rims of ortho-

gneiss pebble zircons from Pennsylvanian conglomerates

Fig. 1. Geological sketch of the Northern Gemeric Unit (modified according to the Geological map of Slovakia, 1:500,000, after Biely et al.

1996 and the Geological map of the Slovenské Rudohorie Mts. — eastern part, 1:50,000, after Bajaník et al. 1984), showing localities of

the studied detrital zircon samples. Abbreviations: LML — Lubenik–Margecany Line; HZL — Hrádok–Železník Line.

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GEOLOGICA CARPATHICA

, 2019, 70, 4, 298–310

(Putiš et al. 2008). Correspondingly, the climax of the Variscan

orogeny in the NGU is indicated by the 355 Ma peak of

the detrital-zircon ages from the post-Tournaisian basin fill

(Vozárová et al. 2013).

The Mississippian (Tournaisian–Visean) turbidite wedges,

supposedly derived from the Variscan suture, represent the fill

of an intrasuture remnant ocean basin. Turbidite deposition

was followed by deposition of latest Visean–Serpukhovian

shallow-water clastics and carbonates. The Mississippian

(Tournaisian–Visean) foredeep and remnant basins have been

correlated across the whole Alpine–Carpathian realm (Nötsch–

Veitsch–Northgemeric Zone, Neubauer & Vozárová 1990;

Veitsch–Nötsch–Szabadbattyan–Ochtiná Zone, Ebner et al.

2008). Although partly syn-orogenic, they also postdate the Late

Devonian/Mississippian climax of the Variscan orogeny. Post-

Variscan deposition includes Upper Bashkirian–Mos covian

fan-delta-shallow-marine to proximal delta and continental

Permian sequences (Rakusz 1932; Rozlozsnik 1935; Rozložník

1963; Bajaník et al. 1981, 1983; Vozárová & Vozár 1988, and

references therein).

Characteristics of the Rakovec Group

The Rakovec Group sequence, which is characterized by

the prevalence of basalts and their pyroclastic rocks, is mainly

associated with fine-grained sediments. Biostratigraphic age

data are not available. The pre-Carboniferous low-grade Rako-

vec Group consists of two lithostratigraphic units (Fig. 1),

(i) the lower Smrečinka Formation and (ii) the upper Sykavka

Formation (Bajaník et al. 1981). The Sykavka Formation is

composed mainly of metabasalts and associated volcaniclas-

tics with rare intercalations of fine-grained metasediments.

Thus, sampling for the zircon selection was focused on the

basal Smrečinka Formation (Fig. 1). This formation is made

up mainly of distal turbiditic metasandstones and metapelites.

Thin slices of metabasalts and related volcaniclastics are pre-

sent near the top of the formation. The Rakovec Group volca-

nic rocks show the geochemical affinity with E-MORB/OIT

basalts (enriched mid-oceanic ridge basalts/oceanic island

basalts) (Ivan 1994, 1997, 2009). In some areas, rhyolite/

dacite bodies occur near the base of the Smrečinka Formation.

U–Pb magmatic zircon from these metadacites yielded an age

of 476 ± 7 Ma (Putiš et al. 2008).

As a result of the lithological differences between the

Sykavka and Smrečinka formations, Ivan (2009) considered

the Smrečinka Formation as a separate lithostratigraphic unit.

Németh (2002) also assigned the Smrečinka Formation to

the upper part of the Gelnica Group (the Hnilec Formation

according to the lithostratigraphy by Németh 2002). But the

mineral composition of the Gelnica Group metasandstones is

distinctly different from the Smrečinka Formation metasand-

stones, which are characterized, in particular, by the lack of

detrital feldspars and the high degree of mineral maturity

metasandstones of the Gelnica Group (Vozárová 1993).

However, the U–Pb analysis of detrital zircons from the over-

stepping Carboniferous–Permian clastic sequences (Vozárová

et al. 2013) confirmed the validity of the original division of

Bajanik et al. (1981) and the legitimacy for incorporation of

the Smrečinka Fm. within the pre-Carboniferous basement of

the NGU zone.

Sample characteristics

One sample has been collected from the Smrečinka For-

mation for zircon dating (Fig. 1). The sample GZ-25 was loca-

ted NNW of Rejdová Village, along a forest road, 550 m above

sea level (GPS coordinates: 48°47.812’ N, 20°17.162’ E).

The Smrečinka Formation metasandstone is composed of

quartz, plagioclase, and relics of deformed and recrystallized

lithic fragments, detrital mica, and rare detrital alkali feldspar

grains. Among quartz grains (~75 % of total) the monocrystal-

line types are dominant, whereas the polycrystalline varieties

are present in a minority. Feldspar grains are relatively com-

mon (~20 % of the total), of these, the plagioclases predomi-

nate. Since the sediments were affected by deformation and

recrystallization reaching greenschist facies metamorphic

conditions, the original lithic fragments are more difficult to

distinguish. Only metasedimentary fragments and fine-grained

detrital white mica were identified (Fig. 2).

The studied metasandstone is characterized by massive,

partly foliated structure. A blastopsammitic texture is charac-

teristic, with clastic grains displaying a variable degree of

pressure solution deformation and a relatively high content of

fine-grained recrystallized matrix (on average 30–40 %),

consisting of fine-grained muscovite, chlorite, quartz and

secon dary albite. According to Dickinson’s criteria (1970)

a con siderable part of the matrix is represented by “pseudo-

matrix”. The process of low-grade recrystallization and deforma-

tion of former clay matrix and sedimentary/metasedimen tary

rock fragments is responsible for “graywackization” of

metasandstones and relative increase of matrix and stable

components in their texture.

Analytical method

Zircons were extracted from the rocks by the standard tech-

nique applying grinding, heavy liquid separation, magnetic

separation and hand-picking. The internal zoning structures

and shapes of the half-sectioned zircon crystals, mounted in

an epoxy resin puck with chips of the TEMORA 1 (zircon

standards derived from the Middledale Gabbroic Diorite;

Black et al. 2003) and 91500 (Wiedenbeck et al. 1995) refe-

rence zircon, were imaged by optical microscopy, back-scat-

tered electrons (BSE) and cathodoluminescence, to guide

analytical spots positioning.

In situ U–Pb analyses were performed using Sensitive High-

Resolution Ion Microprobe (SHRIMP-II) in the Centre of

Isotopic Research (CIR), A.P. Karpinsky Russian Geological

Research Institute at VSEGEI (Vserossijskij naučno-sledo-

vateľskij geologičeskij institut), applying a secondary electron

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multiplier in peak-jumping mode following the procedure

described by Williams (1998) and Larionov et al. (2004).

Primary beam size allowed the analysis of ca. 27×20 µm area.

The 80 µm wide ion source slit, in combination with a 100 µm

multiplier slit, allowed mass-resolution M/ΔM ≥ 5,000 (1 %

valley); hence, all the possible isobaric interferences were resol-

ved. The following ion species were measured in the sequence:

196

(Zr

O) –

204

Pb – background (ca. 204.5 AMU) –

206

Pb –

207

Pb –

208

Pb –

238

U–

248

ThO –

254

UO. Four to five mass-spectra for each

analysis were acquired. Each fifth measurement was carried

out on the TEMORA-1 Pb/U standard (Black et al. 2003).

The 91500 zircon (Wiedenbeck et al. 1995) was applied as

the ‘‘U-concentration’’ standard. The obtained results have

been processed by the SQUID v1.12 (Ludwig 2005a) and

ISOPLOT/Ex 3.22 (Ludwig 2005b) softwares, with decay

constants of Steiger & Jäger (1977). Common lead correction

was done using the measured

204

Pb/

206

Pb ratio. The ages given

in the text, if not additionally specified, are

207

Pb/

206

Pb ages for

zircons older than 1.0 Ga, and

206

Pb/

238

U, for those younger

than 1.0 Ga. The errors are quoted at 1σ level for individual

points and at 2σ 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 % were used. For

inter

pretation purposes, the Probability Density Plot

(ISOPLOT/Ex 3.75, Ludwig 2012) was constructed using

206

Pb/

238

U ages for zircon younger than 1.0 Ga and

207

Pb/

206

ages for zircons older than 1.0 Ga. The Probability Density

Plots include analyses with discordance from 0 % to 15 %.

The Kolmogorov–Smirnov statistical test (K–S) was adopted

from Guynn & Gehrels (2010) and was used for the compari-

son of detrital zircon age distributions.

In this study, we follow the time-scale calibration of the

International Chronostratigraphic Chart (2018-8) (http://www.

stratigraphy.org/ICSchart/ChronostratChart 2018-08.pdf) in

order to compare geochronological data from detrital zircons

with paleontological ages of fossil-bearing sedimentary units

and tectono–thermal events.

Results of zircon dating

49 detrital zircon grains have been analysed from sample

GZ-25. The results of the U–Pb detrital zircon analyses are

provided in the Table 1 and in the Figure 3. The age spectrum

of the detrital zircons is dominated by Neoproterozoic ages

(~56 %). Most of them are Ediacaran in age (~33 %), ranging

between 545 and 635 Ma with major peaks at 547, 598 and

640 Ma on the Probability Density Plot (Fig. 3). Approximately

20 % of analysed zircons yielded Cryogenian ages with a peak

at 640 Ma. Only two grains show late Tonian ages 757 and

774 Ma, whereas the 757 Ma age is related to a xenocrystic

core. Two other grains revealed 0.9–1.0 Ga ages, just strad-

dling the boundary between Tonian and Stenian. Analyses

indicated U contents of 94–575 ppm and Th contents of

74–536 ppm.

232

Th/

238

U ratios range between 0.30–1.49 for all

Neoproterozoic zircons (Table 1). They are most likely to be

results of crystallization from felsic melt composition with

minor mafic influences (Wang et al. 2011). The only exception

is spot 24 of the 633 ± 7 Ma age (Table 1; Fig. 4) with a very

low Th/U ratio of 0.01, indicating a strong post-magmatic or

metamorphic recrystallization process.

A typical feature of the studied Neoproterozoic zircons is

the presence of well-developed growth oscillatory zoning

(Fig. 4). In others, resorption intervals with textural disconti-

nuities have been quite regularly observed, along which the

original zoning is resorbed and succeeded by newly-grown-

zoned zircon. According to Corfu et al. (2003), these resor-

ption intervals reflect intermediate periods of Zr saturation in

the magma, owing to a large-scale mixing singularity, or to

local kinetic phenomena. A special type of zoning is the rare

irregular and patchy texture in solitary zircon grains. This type

of texture may reflect strain experienced by zircons during

Fig. 2. Microtexture and mineral composition of the Smrečinka metasandstones. Abbreviations: Pl — plagioclase; Kfs — feldspar; Qz — quartz;

Lms — lithic fragment; Ser — sericite (fine-grained muscovite in matrix).

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, 2019, 70, 4, 298–310

the final magmatic emplacement or by texture modification

during late- and post-magmatic processes (Corfu et al. 2003

and references therein). Scarce zircon grains with convolute

texture or irregular domains of homogeneous enclaves that cut

the original oscillatory growth zoned texture, also document

the local post-magmatic recrystallization (Fig. 4).

The second major detrital zircon assemblage (17 grains of

the total; 35 %) is represented by Paleoproterozoic ages,

ranging from 1885 to 2132 Ma, whereas 9 concordant grains

yielded a Concordia age of 1892 ± 9 Ma (Fig. 3) corresponding

to the Orosirian. In general, recrystallization features have

been observed in the all studied Paleoproterozoic detrital

zircon grains. Their internal textures are either homogenous

and patchy or convolute. Some of them appear in the form of

xenocrystic cores. The zircon analyses yielded U contents of

28–964 ppm and Th contents of 18–415 ppm.

232

Th/

238

U ratios

1(Age)

spot

206

232

206

Pb*

206

207

Disc.

238

207

Pb*

207

Pb*

206

Pb*

err

ppm ppm

238

ppm

238

206

Pb*

206

Pb*

235

238

corr

0.02

537

236

0.45

48.3

642.3

5.6

617

−4

9.544

0.92

0.0604

0.99

0.872

1.4

0.1048

0.92

.681

0.12

235

179

0.79

23.5

708.7

683

−4

8.605

1.0

0.0623

1.5

0.997

1.8

0.1162

1.0

.571

0.04

274

134

0.50

22.7

592.3

5.8

570

−4

10.39

1.0

0.05901

1.4

0.784

1.7

0.0962

1.0

.599

0.05

203

0.38

17.0

599.2

6.1

570

−5

10.27

1.1

0.0591

1.6

0.794

1.9

0.0974

1.1

.565

0.03

313

360

1.19

45.0

996

997

5.987

1.1

0.0724

0.89

1.667

1.5

0.1670

1.1

.788

0.23

115

0.42

9.29

578.3

6.8

526

−9

10.65

1.2

0.0579

3.2

0.749

3.4

0.0939

1.2

.364

0.03

0.65

29.1

1988

1956

−2

2.768

1.1

0.1200

0.84

5.976

1.4

0.3613

1.1

.786

0.20

0.67

9.04

2071

2046

−1

2.638

1.4

0.1262

1.8

6.59

2.3

0.3788

1.4

.617

0.21

138

0.54

12.1

622

555

−11

9.87

2.0

0.0587

3.0

0.820

3.6

0.1013

2.0

.549

0.41

110

159

1.49

9.19

597.2

6.7

534

−11

10.3

1.2

0.0581

3.1

0.778

3.3

0.0971

1.2

.358

0.29

264

177

0.69

23.0

619.7

599

−3

9.91

1.0

0.0599

2.7

0.833

2.9

0.1009

1.0

.350

0.04

362

165

0.47

31.6

622.4

5.9

614

−1

9.865

0.99

0.0603

1.2

0.843

1.5

0.1014

0.99

.647

0.10

109

0.68

32.0

1900

1921

2.917

1.0

0.1177

0.85

5.560

1.3

0.3427

1.0

.777

0.14

415

388

0.97

34.7

598.1

5.6

583

−3

10.28

0.99

0.0594

1.6

0.797

1.8

0.0972

0.99

.535

0.22

138

107

0.80

40.5

1889

1894

2.936

1.0

0.1159

0.91

5.440

1.4

0.3404

1.0

.743

1.46

118

103

0.90

10.8

643.7

9.8

568

−12

9.52

1.6

0.0590

4.2

0.854

4.5

0.1050

1.6

.360

0.29

153

0.54

14.8

684.7

8.3

637

−7

8.92

1.3

0.0609

2.1

0.941

2.5

0.1121

1.3

.515

0.02

1815 1337

0.76

518.0

1850

1886.7

3.8

3.008

0.88

0.1154

0.21

5.291

0.91 0.3324

0.88

.972

0.05

487

239

0.51

36.9

544.6

4.9

563

11.34

0.94

0.0589

1.1

0.716

1.4

0.0882

0.94

.658

0.14

1700

749

0.46

391.0

1525

2060.8

4.3

3.745

1.1

0.1273

0.24

4.685

1.1

0.2670

1.1

.975

0.01

107

0.92

65.8

3468

3444.6

6.2

−1

1.404

1.0

0.2951

0.4

28.99

1.1

0.7125

1.0

.930

0.04

912

415

0.47

290

2028

2033.4

8.6

2.705

1.1

0.1253

0.48

6.388

1.2

0.3697

1.1

.909

0.01

547

179

0.34

58.6

757.4

7.3

728

−4

8.021

1.0

0.0636

0.79

1.093

1.3

0.1247

1.0

.793

0.10

494

0.01

43.9

633.4

7.5

625

−1

9.69

1.2

0.0606

1.2

0.863

1.7

0.1032

1.2

.728

0.17

206

0.38

22.6

773.6

7.6

750

−3

7.842

1.0

0.0642

1.6

1.129

1.9

0.1275

1.0

.537

0.18

248

210

0.88

22.4

645.1

6.3

599

−7

9.5

1.0

0.0599

1.7

0.869

2.0

0.1053

1.0

.511

0.07

964

286

0.31

261.0

1768

2132.3

5.4

3.169

0.9

0.1326

0.31

5.767

0.95 0.3155

0.9

.945

0.02

105

0.44

63.1

3411

3413.5

9.2

1.434

1.0

0.2892

0.59

27.81

1.2

0.6974

1.0

.866

0.11

137

143

1.08

20.9

1056

1010

−4

5.619

1.0

0.0729

1.5

1.787

1.8

0.1779

1.0

.584

0.20

0.66

21.9

1880

1896

2.952

1.1

0.1160

1.1

5.418

1.5

0.3386

1.1

.724

0.01

404

400

1.02

36.0

634.8

5.9

642

9.664

0.97

0.0611

1.0

0.871

1.4

0.1035

0.97

.690

0.05

471

126

0.28

117.0

1640

2021

3.452

1.2

0.1244

0.86

4.969

1.4

0.2896

1.2

.803

0.17

0.57

4.80

675.5

8.9

699

9.05

1.4

0.0627

3.3

0.955

3.6

0.1105

1.4

.391

0.08

0.73

26.2

1927

1899

−1

2.87

1.1

0.1162

0.96

5.583

1.5

0.3483

1.1

.760

0.06

191

175

0.95

17.0

635.4

6.3

619

−3

9.65

0.0604

1.7

0.863

2.0

0.1036

1.0

.514

0.01

646

358

0.57

193.0

1924

1897.1

−1

2.875

0.9

0.1161

0.33

5.567

0.96 0.3478

0.9

.937

0.35

2078

536

0.27

159

549.5

5.9

525

−4

11.24

1.1

0.0579

0.69

0.7101

1.3

0.0890

1.1

.852

0.06

337

436

1.33

28.5

604.9

601

−1

10.16

1.0

0.0599

1.4

0.813

1.8

0.0984

1.0

.583

0.21

0.99

9.23

665.3

7.9

614

−8

9.2

1.2

0.0603

2.6

0.904

2.9

0.1087

1.2

.434

0.07

413

397

0.99

38.3

660.2

6.1

631

−4

9.272

0.97

0.0608

1.1

0.904

1.5

0.1078

0.97

.649

0.28

0.44

17.9

1573

2002

3.616

1.1

0.1231

1.2

4.693

1.6

0.2764

1.1

.692

0.10

0.76

28.1

1929

1893

−2

2.867

1.1

0.1159

0.94

5.571

1.4

0.3487

1.1

.750

0.09

159

105

0.68

46.5

1892

1885

2.931

1.0

0.1153

0.84

5.422

1.3

0.3411

1.0

.775

0.06

357

327

0.95

32.7

652.6

6.1

634

−3

9.386

0.99

0.0608

1.2

0.894

1.5

0.1065

0.99

.649

0.08

133

107

0.83

38.7

1875

1909

2.962

1.0

0.1169

0.79

5.441

1.3

0.3376

1.0

.792

0.25

128

1.40

8.55

648.1

7.4

652

9.45

1.2

0.0614

2.8

0.895

3.1

0.1058

1.2

.391

0.10

138

109

0.82

41.9

1952

1922

−2

2.827

1.0

0.1177

0.85

5.740

1.3

0.3536

1.0

.767

0.12

575

168

0.30

46.4

578.1

5.4

608

10.66

0.98

0.0601

1.2

0.778

1.5

0.0938

0.98

.635

0.01

740

495

0.69

316.0

2602

2596.4

3.8

2.011

0.9

0.1740

0.23

11.93

0.93 0.4973

0.9

.969

Table 1: U–Pb (SHRIMP) detrital zircon age data from the sample GZ-25. Errors are 1 sigma; Pb

and Pb* indicate the common and radiogenic

portion, respectively. Error in standard calibration was 0.52 % (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.

303

DETRITAL ZIRCONS PROVENANCE OF THE NORTHERN GEMERICUM

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, 2019, 70, 4, 298–310

of the Paleoproterozoic detrital zircons vary from 0.28 to 0.83,

indicating crystallization from a felsic igneous melt (Table. 1).

Only a few zircon grains yielded Neoarchean (2596 ± 6 Ma)

and Paleoarchean (3445 ± 6 and 3413 ± 9 Ma) ages (Table 1).

Discussion

Age data and provenance

The detrital zircon assemblage analysed from the sample

GZ-25 shows a distinct bipolar age distribution (Fig. 3). A pre-

vailing part of the detrital zircons in the GZ-25, metasandstone

sample, displays Neoproterozoic ages spanning between 545

and 709 Ma with a major peak at 547, 598 and 640 Ma, while

Ediacaran zircons are dominant (~33 % of all concordant

grains). Additionally, the GZ-25 sample contains negligible

amounts of Tonian and Tonian/Stenian detritus (only 4 grains),

ranging from 0.75 to 1.0 Ga. The second major detrital zircon

age population is connected with Late Paleoproterozoic ages,

ranging from 1.8 to 2.1 Ga.

The previously published zircon age data from the sample

GZ-24 (Vozárová et al. 2013), also coming from the Smrečinka

Formation, and proved completely identical clusters of the

detrital zircon ages as from the sample GZ-25 (Fig. 5a).

The K–S statistic test confirms that the samples GZ-24 and

GZ-25 demonstrate the statistically significant similarity (at

the 95 % confidence level), with the P value higher then 0.05,

so that they correspond to 0.179 (Table 2).

Taking into account the detrital zircon ages from both sam-

ples (93 spots together), zircon grains show the Neoproterozoic,

with dominance of Ediacaran ages (~60 % of all concordant

grains), which highlights significant peaks at 586 and 629 Ma

at KDE plot (Fig. 5b). The second most represented detrital

zircon ages correspond to Paleoproterozoic (~31 % of all con-

cordant grains) with a distinct peak at 1.90 Ga (Fig. 5b).

This detrital zircon age cluster indicates a significant input

from a Cadomian arc that resides at the periphery of the West

African Craton (WAC) of North Gondwana (Linnemann et al.

2008). The Early Ordovician breakup of the Cadomian crust and

formation of the Rakovec Group sedimentary trough (back-arc

basin) are interpreted as coincident with the crustal-derived

Fig. 3. a — Concordia plot of detrital zircons from the sample GZ-25. b — Selected sector of the Concordia relevant to the most prominent

clusters for the age spectrum from 500 to 800 Ma, with indication of the youngest Concordia age. c — Concordia diagram depicting the

Eburnian detrital zircon population. d — Corresponding Probability Density Plot of detrital zircon ages (according to ISOPLOT/Ex 3.75,

Ludwig 2012).

207

Pb/

235

age (Ma)

207

Pb/

235

207

Pb/

235

206

Pb/

238

206

Pb/

238

206

Pb/

238

304

VOZÁROVÁ, RODIONOV and ŠARINOVÁ

GEOLOGICA CARPATHICA

, 2019, 70, 4, 298–310

felsic volcanism that was identified by Bajaník

et al. (1984) within the Smrečinka Formation,

which were subsequently determined on the basis

of U–Pb zircon data with an age of 476 ± 7 Ma old

(Putiš et al. 2008). A relatively high number of

detrital zircons yielded 1.8–2.1 Ga (Paleoprotero-

zoic, Eburnian) ages. The presence of Eburnian

detrital zircons is usually taken to indicate the

WAC provenance (e.g., Linnemann et al. 2007;

Abati et al. 2012; Gärtner et al. 2013, 2016;

Henderson et al. 2016). The discordant ages from

the samples GZ-24 and GZ-25 appear to define

Fig. 4. Cathodoluminescence images of detrital zircons from the sample GZ-25.

Fig. 5. a — Normalized Probability Density Plot

(according to ISOPLOT/Ex 3.75, Ludwig 2012) of

detrital zircon ages from the Smrečinka metasand-

stones; samples GZ-24 and GZ-25, with discordant fil-

ter from 0 % to 15 %. b — Kernel Density Estimation

for the entire detrital zircon populations, with discor-

dant filter of 10 % (in accordance Vermeesch 2012).

age (Ma)

305

DETRITAL ZIRCONS PROVENANCE OF THE NORTHERN GEMERICUM

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, 2019, 70, 4, 298–310

two clusters, each of which can be roughly coordinated with

a Discordia line with upper intercepts that lie at approximately

1.8 and 2.1 Ga, (Fig. 6). The presence of concordant grains of

similar ages supports the reliability of the upper intercept ages

and suggests that these discordant grains were derived from

Paleo proterozoic (1.8–2.2 Ga) terranes. It may be suggested

that these zircons could have been affected by lead loss during

Early Paleozoic events (lower intercepts at 440 Ma and 480 Ma,

respectively, Fig. 6), which were the most probably connected

with thermal relaxation during crustal extension and the origin

of the Rakovec Group sedimentary trough.

The Smrečinka detrital zircon age spectrum that is domi-

nated by Ediacaran (545–625 Ma) and Paleoproterozoic (1.8–

2.1 Ga) ages, with a minor Archean population (2.5–3.4 Ga),

suggests a linkage with Armorican terranes. Generally, the

Armorican age spectrum contains more Ediacaran ages than

Cryogenian ones, with typical latest age peaks from 540 Ma to

570 Ma of the Cadomian active margin and with a distinctive

Mesoproterozoic age gap (e.g. Fernández-Suárez et al. 2002,

2014; Friedl et al. 2004; Linnemann et al. 2004, 2008; Drost et

al. 2011; Shaw et al. 2014; Dörr et al. 2015; Henderson et al.

2016; Avigad et al. 2018).

Similar detrital zircon assemblages have been found in

the Saxo–Thuringian Zone (Linnemann et al. 2007, 2008),

whereas the zircons overlap with the age and hafnium isotopic

array of the West African Craton (Linnemann et al. 2014). Such

ages, however, are also known from SW Iberia and Brittany

(Fernández-Suárez et al. 2002, 2014), from the Ediacaran sedi-

mentary rocks of the Teplá–Barrandian Complex in the Bohe-

mian Massif (Drost et al. 2011) and in the Armorican Massif

where Cadomian arc sequences are preserved directly with their

Eburnian basement (Icartian gneisses, ~2 Ga) (e.g., D’Lemos

et al. 1990; Chantraine et al. 2001). The observed spectrum of

zircon ages from the Smrečinka Formation meta sandstones cor-

respond to the second event of the Cadomian orogeny, accor-

ding to the interpretation of Linnemann et al. (2008). This was

related to the assumed transition of juvenile to continental

magmatic arc at ~620 Ma, crustal thickening and contamina-

tion by Eburnian basement aged at around 2.0 Ga. This is pro-

ven by the abundance of Paleoproterozoic zircons, as well as

the dominance of Ediacaran ages (average mean at 610±11 Ma)

within the Smrečinka Formation detrital zircons.

Correlation of the detrital zircon age spectra with published

data

The record of Neoproterozoic and Archean zircon ages, is

above all, in the xenocrystic cores of magmatic zircons, mainly

in the Variscan granitoid rocks or in the Cambrian/Ordovician

orthogneisses, coming from the Tatricum and Veporicum

crystalline basements. Generally, they show two age maxima,

either the Neoproterozoic ages ranging from 550 to 660 Ma

or the Paleoproterozoic–Archean set, ranging from ~2.0 Ga

to 3.4 Ga (Poller & Todt 2000; Poller et al 2000, 2001, 2005;

Gaab et al. 2005; Putiš et al. 2008, 2009; Kohút et al. 2009;

Broska et al. 2013; Burda et al. 2013). Rarely, 1.1–1.2 Ga

inherited zircon grains were also described (Broska et al.

2013). An isolated detrital zircon study from mica-schists

of the Western Tatra Mts. was performed by Kohút et al.

(2008). The obtained detrital zircon data yielded mostly

Cambrian/Neoproterozoic ages, in the range of 515–666 Ma.

Several of the oldest cores yielded 1800 and 1980 Ma. Detrital

zircon assemblages from the Late Paleozoic sediments of

the Hro nicum Nappe system determined the age and nature

of their unknown basement and source area (Vozárová et al.

2018). Among the pre-Cambrian detrital zircon grains Edia-

caran ages in the range of 545–612 Ma and Paleo proterozoic–

Neoarchean ages ranging from 1.8 to 2.9 Ga are dominating.

All these published zircon age data indicate a distinct proxi mity

of the source areas and precursor rocks to the crystalline base-

ments of the Central Wes tern Carpathian tectonic units, namely

the Tatri cum, Veporicum and misplaced Hronicum base ments.

However, the Smrečinka detrital zircon age spectrum clearly

shows a similarity with the above- mentioned zircon distribu-

tions and reinforcement of the provenance linkage to the

Cadomian orogenic belt and West African Craton (Fig. 7).

using error in the Cumulative Distribution Function
K-S P-values

D-values

GZ 24

GZ 25

GZ 24

GZ 25

GZ 24

−

0.179

−

0.237

GZ 25

0.179

−

0.237

−

K-S P-values for no error

D-values for no error

GZ 24

GZ 25

GZ 24

GZ 25

GZ 24

−

0.102

−

0.264

GZ 25

0.102

−

0.264

−

using Monte-Carlo
Average K-S P-values

Two std devs. of P-values

GZ 24

GZ 25

GZ 24

GZ 25

GZ 24

−

0.088

−

0.090

GZ 25

0.088

−

0.090

−

Table 2: K–S statistical test of the Smrečinka detrital zircon popu-

lations (samples GZ-24 and GZ-25); table of P- and D-values for

the comparison of studied samples.

Fig. 6. Discordia diagram of the all dated detrital zircons from

the Smrečinka Formation.

207

Pb/

235

206

Pb/

238

306

VOZÁROVÁ, RODIONOV and ŠARINOVÁ

GEOLOGICA CARPATHICA

, 2019, 70, 4, 298–310

Further detrital zircon populations have been

studied from the metasandstones of the Southern

Gemericum (Vozárová et al. 2012), which bor-

ders with the NGU basement. The major part of

the Southern Gemeric Unit (SGU) is formed by

the low-grade Early Paleozoic volcanic–sedi-

mentary sequence of the Gelnica Group and

a pre- Permian low-grade complex of the Štós

Formation. The mutual contact of these rock

complexes is tectonic, along a shallow north-ver-

ging thrust plane, which is documented by deep

seismic profile data (Vozár et al. 1995). Both

these pre-Permian low-grade crystalline comple-

xes are unconformably overstepped by the Per-

mian continental sediments of the Gočaltovo

Group (Bajaník et al. 1983, 1984). The dataset of

concordant 46 detrital zircon ages from the SGU

basement, which were combined with the 20 xeno -

crystic cores from the Early Paleozoic metavol-

canics, yielded the three main zircon age populations. They

are: (i) Neo pro terozoic in the range of 560–870 Ma, with

the main peaks at 630 and 700 Ma; (ii) Tonian–Stenian in

the range of 0.9–1.1 Ga; (iii) Paleo proterozoic/Archean ran-

ging from 1.75 to 3.2 Ga.

The main difference among the Smrečinka Fm. and the SGU

zircon populations, are manifested by the presence of Tonian–

Stenian ages in the range of 0.9 and 1.1 Ga, as well as by

the shifting of the prevalent part of Neoproterozoic zircon

ages to the Cryogenian, with peaks at 630 and 700 Ma in

the SGU basement (Fig. 8). This zircon age span indicates

derivation of Pan-African sources from within the Saharan

Metacraton.

Thus, the main difference between the low-grade NGU and

SGU Lower Paleozoic basements resulted from their different

provenances, as well as from their diverse position along

the North Gondwana margin, which was induced by the Cado-

mian arc and West African Craton provenance for the NGU

basement and the Pan-African Belt–Saharan Metacraton pro-

venance for the SGU basement (Fig. 7).

Conclusions

Forty-nine new U–Pb detrital zircon data from the Smre-

činka Fm. metasandstones are presented. The Smrečinka Fm.

metasandstones belong to the basal part of the Rakovec Group

that is a part of the Northern Gemericum basement. These

zircon age data were combined with forty-four previously

published detrital zircon ages, assuring the provenance of this

region from the N-Gondwanan realm, as well as to compare

the Smrečinka zircon population to the zircon ages from

Fig. 8. Correlation plots of normalized Probability Density curves (according to

ISOPLOT/Ex 3.75, Ludwig 2012) from Early Paleozoic detrital zircon assemblages

of the Northern Gemericum and the Southern Gemericum units. The probability

density curves include analyses with discordance between 0 % and 15 %. Detrital

zircon age data are taken from the present paper and from Vozárová et al. (2012,

2013).

Fig. 7. Early Ordovician plate-tectonic reconstruction showing presumed location of the NGU and SGU terranes (yellow stars) in the peri-Gond-

wana realm (modified from von Raumer et al. 2003). Abbreviations: BV – Bruno-Vistulikum; SX – Saxothuringia; SM – Serbo-Macedonian;

MD – Moldanubia; Am – Armorica; PE – Penninic; AA – Austro-Alpine; IA – Intra-Alpine; DH – Dinarides-Hellenides. Approximate position

of the West African Craton (WAC) and the Sahara Metacraton (SMC) according to Meert & Lieberman (2008). Dashed line – future opening

of Palaeotethys.

Age (Ma)

307

DETRITAL ZIRCONS PROVENANCE OF THE NORTHERN GEMERICUM

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, 2019, 70, 4, 298–310

the other parts of the Western Carpathian crystalline base-

ments. The results can be summarized as follows:

• The studied assemblages of U–Pb detrital zircon ages show

a significant bimodal distribution, which is dominated by

Ediacaran (545–625 Ma) and Paleoproterozoic (1.8–2.1 Ga)

ages, with a smaller Archean population (2.5–3.4 Ga).

• In general, this dispersal of detrital zircon ages suggests

a linkage with Armorican terranes, which are characterized

by derivation from the Cadomian arc which lay on the peri-

phery of the West African Craton of North Gondwana. Rewor-

king of the Eburnian crust is characteristic as is documented

by the presence of the 1.8–2.1 Ga detrital zircons.

• The acquired detrital zircon assemblages enable us to

correlate the source area of the Rakovec Group, including

the Smrečinka Fm. metasedimentary rocks with the equiva-

lent provenances for the Tatricum and Veporicum, as well as

the displaced Hronicum basement rocks.

• The discordant ages can be roughly coordinated with

a Discordia line with the upper intercept lying at 1.8 and

2.1 Ga, and the lower intercept at 440 Ma and 480 Ma,

respectively. The presence of concordant grains of similar

age supports the reliability of the upper intercept ages and

suggests that these discordant grains were derived from

Paleoproterozoic (1.8–2.2 Ga) terranes. It may be suggested

that these zircons could have been affected by lead loss

during Ordovician events. These were most probably con-

nected with thermal relaxation during crustal extension and

the origin of the Rakovec Group sedimentary trough.

Acknowledgements: The financial support of the Slovak

Research and Development Agency (project ID: APVV-0546-

11) is gratefully appreciated. The authors would like to thank

F. Neubauer and Z. Németh for constructive reviews and for

their helpful and critical comments which led to significant

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 at west from the Štítnik Fault. Geol. Práce,

Správy 57, 339–348 (in Slovak).

Allen M.B., Morton A.C., Fanning C.M., Ismail-Zadeh A.J. &

Kroonenberg S.B. 2006: Zircon age constraints on sediment

provenance in the Caspian region. J. Geol. Soc., London 163,

647–655.

Andrusov D. 1959: Geology of the Czechoslovak Western Carpa-

thians, 2

part. VEDA Publishing House, Bratislava, 1–376

(in Slovak).

Andrusov D. 1968: Grundriss der Tektonik der Nördlichen Karpaten.

Slovak Academy of Sciences Publ. House, Bratislava, 1–188.

Avigad D., Gerdes A., Morag N. & Bechstadt T. 2012: Coupled

U–Pb–Hf of detrital zircons of Cambrian sandstones from

Morocco and Sardinia: implications for provenance and Precam-

brian crustal evolution of north Gondwana. Gondwana Res. 21,

690–703.

Avigad D., Rossi Ph., Gerdes A. & Abdo A. 2018: Cadomian

metasediments and Ordovician sandstones from Corsica:

detrital zircon U–Pb–Hf constraints on their provenance and

paleogeo graphy. Int. J. Earth Sci. (Geol. Rundsch.) 107,

2803–2818.

Bajaník Š., Vozárová A. & Reichwalder P. 1981: Lithostratigraphic

classification of Rakovec Group and Late Paleozoic sediments

in the Spišsko-gemerské rudohorie Mts. Geol. Práce, Správy 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. 1984: Geological map of the Slovenské

rudohorie Mts. — eastern part, 1:50,000. D. Štúr Inst. Geol.,

Bratislava.

Balintoni I., Balica C., Ducea N.M., Hann P.H. & Şabliovschi V.

2010: The anatomy of a Gondwana terrane: The Neoprotero-

zoic–Ordovician basement of the pre-Alpine Sebeş-Lotru com-

posite terrane (South Carpathians, Romania). Gondwana Res.

17, 561–572.

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. 1996: Geological map of Slovakia.

Ministry of the Environment of Slovak Republic, Geological

Survey of 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.

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. 2013: Geochronology and petro-

genesis of granitoid rocks from the Goryczkowa Unit, Tatra

Mountains (Central Western Carpathians). Geol. Carpath. 64, 6,

419–435.

Chantraine J., Egal E., Thiéblemont D., Le Goff E., Guerrot C.,

Ballèvre M. & Guennoc P. 2001: The Cadomian active margin

(North Armorican Massif, France): a segment of the North

Atlantic Panafrican belt. Tectonophysics 331, 1–18.

Corfu F., Hanchar J.M., Hoskin P.W.O. & Kinny P. 2003: Atlas Zircon

Textures. In: Hanchar J.M. & Hoskin P.W.O. (Eds.): Zircon.

Mineralogical Society of America and Geochemical Society.

Rev. Min. Geochem. 53, 469–500.

Dallmayer 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

Ar/

Ar mineral and

whole rock data. Eclogae Geol. Helv. 89, 203–227.

Dallmayer R.D., Németh Z. & Putiš M. 2005: Regional tectonother-

mal events in Gemericum and adjacent units (Western Carpa-

thians, Slovakia): Contribution by

Ar/

Ar dating. Slovak Geol.

Mag. 11, 2–3, 155–163.

Dickinson W.R. 1970: Interpreting detrital modes of graywacke and

arkose. J. Sediment. Petrol. 40, 695–707.

Dickinson W.R. & Gehrels G.E. 2003: U–Pb ages of detrital zircon

from Permian and Jurassic aeolian sandstones of the Colorado

Plateau, USA: paleogeographic implications. Sediment. Geol.

163, 29–66.

Dickinson W.R. & Gehrels G.E. 2008: U–Pb ages of detrital zircons

in relation to paleogeography: Triassic paleodrainage networks

and sediment dispersal across southwest Laurentia. J. Sediment.

Res. 78, 12, 745–764.

308

VOZÁROVÁ, RODIONOV and ŠARINOVÁ

GEOLOGICA CARPATHICA

, 2019, 70, 4, 298–310

D’Lemos R.S., Strachan R.A. & Topley C.G. 1990: The Cadomian

orogeny in the North Armorican Massif: a brief review. In:

D’Lemos R.S., Strachan R.A. & Topley C.G. (Eds.): The Cado-

mian orogeny. Geol. Soc. Spec. Publ. 51, 3–12.

Dörr W., Zulauf G., Gerdes A., Lahaye Y. & Kowalczyk G. 2015:

A hidden Tonian basement in the eastern Mediterranean: age

constraints from U-Pb data of magmatic and detrital zircons of

the external Hellenides (Crete and Peloponnesus). Precambr.

Res. 258, 83–108.

Drost K., Gerdes A., Jeffries T., Linnemann U. & Storey C. 2011:

Provenance of Neoproterozoic and early Paleozoic siliciclastic

rocks of the Teplá–Barrandian unit (Bohemian Massif): Evi-

dence from U–Pb detrital zircon ages. Gondwana Res. 19, 1,

213–231.

Ebner F., Vozárová A., Kovács S., Kräutner H-G., Krstić B., Szeder-

kényi T., Jamićić D., Balen D., Belak M. & Trajanova M. 2008:

Devonian–Carboniferous pre-flysch and flysch environments in

the Circum Pannonian Region. Geol. Carpath. 59, 2, 159–195.

Fedo C.M., Sircombe K.N. & Raibird R.H. 2003: Detrital zircon ana-

lysis of the sedimentary record. Rev. Mineral. Geochem. 53,

277–303.

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.

Fernández-Suárez J., Gutiérrez-Alonso G., Pastor-Galán D., Hofmann

M., Murphy J.B. & Linnemann U. 2014: The Ediacaran–Early

Cambrian detrital zircon record of NW Iberia: possible sources

and paleogeographic constraints. Int. J. Earth Sci. (Geol.

Rundsch.) 103, 5, 1335–1357.

Friedl G., Finger F., Paquette J.L., von Quadt A., McNaughton N.J. &

Fletcher I.R. 2004: Pre-Variscan geological events in the Aus-

trian part of the Bohemian Massif deduced from U–Pb zircon

ages. Int. J. Earth Sci. 93, 802–823.

Froitzheim N., Plašienka D. & Schuster R. 2008: Alpine tectonics

of the Alps and Western Carpathians. In: McCann T (Ed.):

The Geo logy of Central Europe. Volume 2: Mesozoic and Ceno-

zoic. Geological Society Publishing House, London, 1141–1232.

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.

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.

Gehrels G.E., Dickinson W.R., Ross G.M., Stewart J.H. & Howell

D.G. 1995: Detrital zircon reference for Cambrian to Triassic

miogeoclinal strata of western North America. Geology 23,

831–834.

Gehrels G.E., Dickinson W.R., Reley B.C.D., Finney S.C. & Smith

M.T. 2000: Detrital zircon geochronology of the Roberts Moun-

tains allochton. In: Soreghan M.J. & Gehrels G.E. (Eds.): Paleo-

zoic and Triassic Paleogeography and Tectonics of Western

Nevada and Northern California. Geol. Soc. Amer. Spec. Papers,

347, 19–42.

Guynn J. & Gehrels G.E. 2010: Comparison of detrital zircon age

distribution Using the K-S test. 1–16, http://sites.google.com/a/

laserchron.org/laserchron/home Accessed 8 Mar 2017

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 hafnium

isotopic fingerprints in Avalonia, Iberia and the Armorican Ter-

ranes. Tectonophysics 681, 278–304.

Hervé F., Fanning C.M. & Pankhurst R.J. 2003: Detrital zircon age

patterns and provenance of the metamorphic complexes of

southern Chile. J. South Amer. Earth Sci. 16, 107–123.

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.

International Commission on Stratigraphy 2018: International Chro-

nostratigraphic Chart v. 2018/08. http://www.stratigraphy.org/

ICSchart/ChronostratChart 2018-08.pdf

Ivan P. 1994: Early Paleozoic of the Gemeric Unit (Inner western Car-

pathians): Geodynamic setting as inferred from metabasalts geo-

chemistry data. Mitt. Öster. Geol. Gesell. 86, 3– 31.

Ivan P. 1997: Rakovec and Zlatník Formations: two different relics of

the pre-Alpine back-arc basin crust in the Central Western Car-

pathians. In: Grecula P., Hovorka D. & Putiš M. (Eds.): Geolo-

gical Evolution of the Western Carpathians. Mineralia Slovaca,

Monograph, Bratislava, 281–288.

Ivan P. 2009: Early Palaeozoic basic volcanism of the Western Car-

pathians: geochemistry and geodynamic position. Acta Geolo-

gica Universitatis Comenianae, Monographic serie, Comenius

University, Bratislava, 7–110 (in Slovak).

Kohút M., Poller U., Gurk C. & Todt W. 2008: Geochemistry and

U–Pb detrital zircon ages of metasedimentary rocks of the Lower

Unit, Western Tatra Mountains (Slovakia). Acta Geol. Pol. 58 ,

4, 371–384.

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.

Kolodner K., Avigad D., McWilliams M., Wooden J.L., Weissbrod T.

& Feinstein S. 2006: Provenance of north Gondwana Cambrian–

Ordovician sandstones: U-Pb SHRIMP dating of detrital zircons

from Israel and Jordan. Geol. Mag. 143, 367–391.

Larionov A.N., Andreichev V.A. & Gee D.G. 2004: The Vendian

alkaline igneous suite of northern Timan: ion microprobe U–Pb

zircon ages of gabbros and syenite. In: Gee D.G. & Pease V.

(Eds.): The Neoproterozoic Timanide Orogen of Eastern Baltic.

Mem. Geol. Soc. London 30, 69–74.

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 Gond-

wana? 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. Amer. Spec. Pap. 423,

61–96.

Linnemann U., Pereira F., Jeffries T.E., Drost K. & Gerdes A. 2008:

The Cadomian Orogeny and the opening of the Rheic Ocean:

The diachrony of geotectonic processes constrained by LA-ICP-

MS U–Pb zircon dating (Ossa-Morena and Saxo–Thuringian

Zones, Iberian and Bohemian Massifs). Tectonophysics 461, 21–43.

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.

309

DETRITAL ZIRCONS PROVENANCE OF THE NORTHERN GEMERICUM

GEOLOGICA CARPATHICA

, 2019, 70, 4, 298–310

Lorenz H., Gee D.G. & Simonetti A. 2008: Detrital zircon provenance

of the Late Neoproterozoic and Paleozoic succession on Sever-

naya Zemlya, Kara Shelf: a tie to Baltica. Norw. J. Geol. 88,

235–258.

Ludwig K.R. 2005а: SQUID 1.12 A Userʼs Manual. A Geochro no -

logical Toolkit for Microsoft Excel. Berkeley Geochronology

Centre Special Publication, 1–22. http://www.bgc.org/

klprogram menu.html

Ludwig K.R. 2005b: Userʼs Manual for ISOPLOT/Ex 3.22. A Geo-

chronological Toolkit for Microsoft Excel. Berkeley Geochro-

nology Centre Special Publication, 1–71. 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

Centre Special Publication No. 5, 1–71. http://www.bgc.org/

isoplot.html

Maheľ M. 1986: Geological structure of the Czechoslovak Carpa-

thians, Part 1: Paleoalpine units. Veda Publ. House, Bratislava,

1–503 (in Slovak).

McLennan S.M., Bock B., Compston W., Hemming S.R. & McDaniel

D.K. 2001: Detrital zircon geochronology of Taconian and Aca-

dian foreland sedimentary rocks in New England. J. Sediment.

Res. 71, 305–307.

Meert J.G. & Lieberman B.S. 2008: The Neoproterozoic assembly of

Gondwana and its relationship to the Ediacaran–Cambrian radia-

tion. Gondwana Res. 14, 5–21.

Meinhold G. & Frei D. 2008: Detrital zircon ages from the islands of

Inousses and Psara, Aegean see, Greece: constraints on deposi-

tional age and provenance. Geol. Mag. 145, 886–891.

Mueller P.A., Foster D.A., Mogk D.W., Wooden J.L., Kamenov G.D.

& Vogl J.J. 2007: Detrital mineral chronology of the Uinta

Mountain Group: implication for the Grenville flood in

south-western Laurentia. Geology 35, 431–434.

Németh Z. 2002: Variscan suture zone in Gemericum: Contribution to

reconstruction of geodynamic evolution and metallogenetic

events of Inner Western Carpathians. Slovak Geol. Mag. 8, 3–4,

247–257.

Neubauer F. & von Raumer J.F. 1993: The Alpine basement: linkage

between west-European Variscides and Alpine-Mediterranean

Mountain Belt. In: von Raumer J.F. & and Neubauer F. (Eds.):

The pre-Mesozoic geology in the Alps. Springer, Berlin, 640–

663.

Neubauer F. & Vozárová A. 1990: The Noetsch–Veitsch–Northge-

meric Zone of Alps and Carpathians: Correlation, paleogeo-

graphy and significance for Variscan orogeny. In: Minaříková D.

& Lobitzer H. (Eds.): Thirty years of geological cooperation

between Austria and Czechoslovakia. Federal Geol Surv.,

Vienna, 167–171.

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.

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.

Poller U., Todt W., Kohút M. & Janák M. 2001: Nd, Sr, Pb isotope

study of the Western Carpathians: implications for Palaeozoic

evolution. Schweiz. Mineral. Petrogr. Mitt. 81, 15–174.

Poller U., Kohút M., Anders B. & Todt W. 2005: Multistage geo-

chronological evolution of the Velká Fatra Mountains —

a combined TIMS and ion-microprobe study on zircons. Lithos

82, 113–124.

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.

2009: 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.

Rakusz Gy. 1932: Die oberkarbonischen Fosilien von Dobšiná und

Nagyvisnyó. Geol. Hungarica, serie Paleont. 8, 1–219.

Rozlozsnik P. 1935: Die geologischen Verhältnisse der Gegend von

Dobšiná. Geol. Hungarica, Serie Geologie, 5, 1–118.

Rozložník L. 1963: Basic volcanites in the Dobšiná Carboniferous

facies: Geol. Práce Správy 27, 35–48 (in Slovak).

Shaw J., Guttiérez-Alonso G., Johnston S.T. & Pastor-Galán D. 2014:

Provenance variability along the Early Ordovician north Gond-

wana margin: Paleogeographic and tectonic implications of

U–Pb detrital zircon ages from the Armorican Quartzite of the

Iberian Variscan belt. Geol. Soc. Amer. Bull., doi:10.1130/

B30935.1

Schmid S.M., Bernoulli D., Fügenschuh B., Matenco L., Schefer S.,

Schuster R., Tischler M. & Ustaszewski K. 2008: The Alpine–

Carpathian–Dinaridic orogenic system: correlation and evolu-

tion of tectonic units. Swiss J. Geosci. 100, 139–183.

Spencer C.J., Kirkland C.L. & Taylor R.J.M. 2016: Strategies towards

statistically robust interpretations of in situ U–Pb zircon geo-

chronology. Geoscience Frontiers 7, 581–589.

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 Správy 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.

Stewart J.H., Gehrels G.E., Barth A.P., Link P.K., Christie-Blick N. &

Wrucke C.T. 2001: Detrital zircon provenance of Mesoprotero-

zoic to Cambrian arenites in the western United States and north-

western Mexico. Geol. Soc. Am. Bull. 113, 1343–1356.

Ustaömer P.A., Ustaömer T., Gerdes A. & Zulauf G. 2011: Detrital

zircon ages from a Lower Ordovician quartzite of the Istambul

exotic terrane (NW Turkey): evidence for Amazonian affinity.

Int. J. Earth Sci. (Geol. Rundsch.) 100, 23–41.

Vermeesch P. 2012: On the visualization detrital age distributions.

Chem. Geol. 312–313, 190–194.

von Raumer J.E., Stampfli G.M. & Bussy F. 2003: Gondwana-deri-

ved microcontinents — the constituents of the Variscan and

Alpine collisional orogens. Tectonophysics 36, 7–22.

Vozár J., Tomek Č. & Vozárová A 1995: Deep seismic profile G: geo-

logical interpretation (Western Carpathians, Slovakia). PAN-

CARDI Conference Abstract, Stará lesná, 8–12.

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. 1993: Provenance of Gelnica Group metasandstones and

relationship to paleotectonics of the sedimentary basin. Západné

Karpaty, sér Min Petr Metalog Geoch 16, 7-54 (in Slovak with

English summary).

Vozárová A. & Vozár J. 1988: Late Paleozoic in West Carpathians.

Monogr, D. Štúr. Inst. Geol., Bratislava, 1–314.

Vozárová A. & Vozár J. 1996: Terranes of the West Carpathian–North

Pannonian domain. Slovak Geol. Mag. 1, 65–85.

Vozárová A., Frank W., Kráľ J. & Vozár J. 2005:

Ar/

Ar dating of

detrital mica from the Upper Paleozoic sandstones in the Wes-

tern Carpathians (Slovakia). Geol. Carpath. 56, 6, 463–472.

310

VOZÁROVÁ, RODIONOV and ŠARINOVÁ

GEOLOGICA CARPATHICA

, 2019, 70, 4, 298–310

Vozárová A., Šmelko M., Paderin I. & Larionov A. 2012: Permian

volcanics in the Northern Gemericum and Bôrka Nappe

system: U–Pb zircon dating and implication to geodynamic

evolution (Western Carpathians, Slovakia). Geol. Carpath. 63,

191–200.

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 Ge-

mericum (Western Carpathians, Slovakia). J. Sediment. Res. 83,

915–927.

Vozárová A., Larionov A., Šarinová K., Vďačný M., Lepekhina E.,

Vozár J. & Lvov P. 2018: Detrital zircons from the Hronicum

Carboniferous–Permian sandstones (Western Carpathians,

Slovakia): depositional age and provenance. Int. J. Earth Sci.

(Geol. Rundsch.) 107, 1539–1555.

Wang X., Griffin W.L., Chen J., Huang P. & Li X. 2011: U and Th

contents and Th/U ratios of zircon in felsic and mafic magmatic

rocks: improved zircon–melt distribution coefficient. Acta Geol.

Sinica (English Edition) 85, 1, 164–174.

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. Geostandard 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.): Applica-

tions of microanalytical techniques to understanding minerali-

zing processes. Rev. Econ. Geol. 7, 1–35.

Zajzon N., Szabó Zs., Weisburg G.T. & Jeffries E.T. 2011: Multiple

provenance of detrital zircons from the Permian-Triassic boun-

dary in the Bükk Mts., Hungary. Int. J. Earth Sci. (Geol.

Rundsch.) 100, 125–138.