GeolCarp_Vol68_No4_350

GEOLOGICA CARPATHICA

, AUGUST 2017, 68, 4, 350 – 365

doi: 10.1515/geoca-2017-0024

www.geologicacarpathica.com

Age and microfacies of oceanic Upper Triassic radiolarite

components from the Middle Jurassic ophiolitic mélange

in the Zlatibor Mountains (Inner Dinarides,

Serbia) and their provenance

HANS-JÜRGEN GAWLICK



, NEVENKA DJERIĆ

, SIGRID MISSONI

, NIKITA YU. BRAGIN

RICHARD LEIN

, MILAN SUDAR

and DIVNA JOVANOVIĆ

University of Leoben, Department for Applied Geosciences and Geophysics: Petroleum Geology, Peter-Tunner-Str. 5,

8700 Leoben, Austria;



gawlick@unileoben.ac.at

University of Belgrade, Faculty of Mining and Geology, Department of Palaeontology, Kamenička St. 6, P.O.Box 62, 11120 Belgrade-35, Serbia

Geological Institute, Russian Academy of Sciences, Pyzhevsky 7, 119017 Moscow, Russia

Centre of Earth Sciences, University of Vienna, Althanstr. 14, 1090 Vienna, Austria

Serbian Academy of Sciences and Arts, Knez Mihaila 35, 11000 Belgrade, Serbia

Geological Survey of Serbia, Rovinjska 12, 11000 Belgrade, Serbia

(Manuscript received November 25, 2016; accepted in revised form June 6, 2017)

Abstract: Oceanic radiolarite components from the Middle Jurassic ophiolitic mélange between Trnava and Rožanstvo

in the Zlatibor Mountains (Dinaridic Ophiolite Belt) west of the Drina–Ivanjica unit yield Late Triassic radiolarian ages.

The microfacies characteristics of the radiolarites show pure ribbon radiolarites without crinoids or thin-shelled bivalves.

Beside their age and the preservation of the radiolarians this points to a deposition of the radiolarites on top of the oceanic

crust of the Neo-Tethys, which started to open in the Late Anisian. South of the study area the ophiolitic mélange

(Gostilje–Ljubiš–Visoka–Radoševo mélange) contains a mixture of blocks of 1) oceanic crust, 2) Middle and Upper

Triassic ribbon radiolarites, and 3) open marine limestones from the continental slope. On the basis of this composition

we can conclude that the Upper Triassic radiolarite clasts derive either from 1) the younger parts of the sedimentary

succession above the oceanic crust near the continental slope or, more convincingly 2) the sedimentary cover of ophiolites

in a higher nappe position, because Upper Triassic ribbon radiolarites are only expected in more distal oceanic areas.

The ophiolitic mélange in the study area overlies different carbonate blocks of an underlying carbonate-clastic mélange

(Sirogojno mélange). We date and describe three localities with different Upper Triassic radiolarite clasts in a mélange,

which occurs A) on top of Upper Triassic fore-reef to reefal limestones (Dachstein reef), B) between an Upper Triassic

reefal limestone block and a Lower Carnian reef limestone (Wetterstein reef), and C) in fissures of an Upper Triassic

lagoonal to back-reef limestone (Dachstein lagoon). The sedimentary features point to a sedimentary and not to a tectonic

emplacement of the ophiolitic mélange (= sedimentary mélange) filling the rough topography of the topmost

carbonate-clastic mélange below. The block spectrum of the underlying and slightly older carbonate-clastic mélange

points to a deposition of the sedimentary ophiolitic mélange east of or on top of the Drina–Ivanjica unit.

Keywords: Neo-Tethys, trench-like basins, synorogenic deposition, evolving thrust belt, Triassic palaeogeography.

Introduction

Latest Ladinian and Late Triassic ribbon radiolarites are of

special interest, because only these sediments undoubtedly

represent the original sedimentary cover of the Neo-Tethys

ocean crust (for review see Gawlick & Missoni 2015). In con-

trast, Late Anisian to early Late Ladinian radiolarites were

deposited on ocean floor or on subsided continental margins,

where these Late Anisian to early Late Ladinian radiolarites

were widespread and also formed in relatively shallow water

depths (Gawlick et al. 2012 a; Gawlick & Missoni 2015).

Therefore, Late Anisian to early Late Ladinian radiolarites

either derive from the distal shelf to continental slope region

or the oceanic realm, as also expressed in a characteristic

microfacies (e.g., Gawlick & Missoni 2015; Gawlick et al.

2016 a, b). In contrast, latest Ladinian to Rhaetian ribbon

radio larites were absent in continental-margin settings and

clearly indicate deposition on the ocean floor (Krische et al.

2014; Gawlick & Missoni 2015). The absence of ribbon radio-

larites on the continental margin is due to the fact that supply

from shallow-water carbonate ramps and platforms led to the

accumulation of a thick pile of carbonate mud on the distal

shelf and partly even in the proximal oceanic domain (Gawlick

& Böhm 2000). This is valid for the late Middle and Late

Triassic except the Julian stage. Accordingly, radiolarites of

this age can only be expected in more distal oceanic areas

(Gawlick et al. 2008; Krische et al. 2014).

Synorogenic erosion and deposition is a characteristic

feature of evolving thrust belts. The structures of the Jurassic

orogeny in the eastern Mediterranean mountain chain are

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often masked by the younger and polyphase tectonic motions

(Schmid et al. 2008). In addition, synorogenic sedimentary

basin fills or mass transport deposits in trench-like basins in

front of a propagating nappe stack, are commonly overprinted

by multiple deformational events or reworked by tectonics,

showing the typical features of a mélange. To distinguish

a tectonic from a sedimentary mélange (Hsü 1968, 1974;

Gawlick & Frisch 2003; Gawlick et al. 2008, 2012b, 2016 a;

Festa et al. 2010 a, b; Plašienka 2012) is especially compli-

cated in cases, in which the synorogenic basin fills were incor-

porated into the nappe stack becoming sheared forming

olisto stromal carpets (Festa et al. 2016).

To unravel the depositional characteristics of synorogenic

sedimentary successions (mélanges) accompanied by compo-

nent analysis provide an excellent possibility to reconstruct

the geodynamic history of an evolving mountain belt.

Component analyses of conglomerates, breccia layers or tur-

bidite beds are a common tool in sedimentary geology. One

classical approach is provenance analysis, the reconstruction

of the source area from the clast spectrum of the re-sedimented

rocks (Blatt 1967; Zuffa 1980, 1985; Lewis 1984). Whereas

the detailed provenance analyses of siliciclastic material is

common, provenance analyses of carbonate or radiolarite

clasts in conglomerates or breccias remain rare (Gawlick et al.

2008, 2009 a, 2015, 2016 a, b; Krische et al. 2014). For reliable

results, a macroscopic description of the incorporated clasts

has to be combined with microfacies analyses (Flügel 2004)

and age dating. Carbonate and radiolarite clasts should be

dated by their microfossil content, if possible. Such analyses

provide the possibility of an exact reconstruction of the prove-

nance area. The proof of a single component may change plate

tectonic and palaeogeographic reconstructions substantially.

Of special interest and still controversial is the original

emplacement and genesis of the ophiolitic mélange in the

Inner Dinarides, especially in the Dinaridic Ophiolite Belt.

Three different possibilities are discussed in the moment:

A) a tectonic mélange formed on the base of the overriding

ophiolite sheets of the Zlatibor mafic and ultramafic massifs,

B) a sedimentary mélange formed in front of the obducted

ophiolites in trenches or foredeeps, or C) an original sedimen-

tary olistostrome and mass transport dominated deep-water

basin fill in front of an advancing nappe stack later incorpo-

rated in the nappe stack forming an olistostromal carpet below

the overthrusted units (Fig. 1).

Radiolarite and carbonate clasts from the Gostilje–Ljubiš–

Visoka–Radeševo ophiolitic mélange south of our study area

were recently investigated in detail by Gawlick et al. (2016 b).

The age of the ophiolitic mélange was dated as late Middle to

early Late Jurassic by means of radiolarians. The components

in the mélange were attributed to oceanic and distal continen-

tal slope provenance. The mélange was attributed to be a sedi-

mentary mélange, but the question of exact timing of its

emplacement in its present geographical position in the

Dinaridic Ophiolite Belt west of the Drina–Ivanjica unit could

not be solved. At present it is commonly believed that ophio-

lite obduction on the Adria margin started in the Late (latest)

Jurassic and that the ophiolite nappes including their under-

lying mélange were emplaced in the area of the Dinaridic

Ophiolite Belt around the Jurassic/Cretaceous-boundary or the

Early Cretaceous (Djerić et al. 2007; Schmid et al. 2008).

However, Gawlick et al. (2009 b, 2016 b) proved that the onset

of obduction onto the Adria continental margin of the Inner

Dinarides was Middle Jurassic, and therefore contempora-

neous with the onset of obduction in the Albanides (Gawlick

et al. 2008) or Hellenides (Baumgartner 1985; Ozsvárt et al.

2012; Ferriére et al. 2016). Gawlick et al. (2016 b) speculated

therefore that ophiolite obduction started in the middle Middle

Jurassic, affecting at that time the most distal parts of the Adria

margin, and continued until the early Late Jurassic reaching at

that time the area of the Drina–Ivanjica unit. Later, in the

Latest Jurassic to earliest Cretaceous, new tectonic motions

probably related to mountain uplift (Missoni & Gawlick

2011a, b) resulted in the ongoing westward transport of the

ophiolite nappe stack including the underlying mélanges.

The final emplacement of the mélanges and the nappes in the

area of the Dinaridic Ophiolite Belt, meaning to the west of the

Drina–Ivanjica unit is therefore much younger than the forma-

tion of the mélanges.

On basis of the commonly accepted reconstruction of the

Triassic to Early Jurassic shelf (passive continental margin)

(compare Gawlick et al. 1999, 2008; Haas et al. 2011; Kovács

et al. 2011) and the reconstruction of the westward propaga-

ting nappe stack during Middle to early Late Jurassic times

(Gawlick et al. 2008, 2012 b; Schmid et al. 2008) we present

here new data which clearly indicate, that 1) the deposition of

the ophiolitic mass transport deposits on top of a carbonate-

clastic trench-like basin fill with material from the back-reef to

fore-reef facies belt of the destroyed Triassic-Jurassic passive

margin of Adria took place in late Middle to early Late Jurassic

times in 2) an area east of or on top of the Drina–Ivanjica unit.

A primary sedimentary origin of the ophiolitic mélange

today below the ophiolites of Zlatibor Mountains can be

proven. In addition, the earliest stage of the deposition of such

a sedimentary ophiolitic mélange above an older trench-like

basin filled with km-sized slide-blocks on top is described

here for the first time. The earliest mass transport deposits

reflecting synorogenic erosion of the advancing ophiolite

nappe stack fill the rough topography of the older basin fill.

Geological setting

The study area is located west of the Drina–Ivanjica unit in

the most eastern part of the Dinaridic Ophiolite Belt south of

Užice (Fig. 2a). This part of the Dinaridic Ophiolite Belt con-

sists of a series of different mélanges or olistostromal bodies

(Fig. 2b), which should derive from the Drina–Ivanjica unit,

first described by Dimitrijević (1982), but in a different

meaning: Dimitrijević (1982) interpreted the reworked car-

bonate clasts as part of the original sedimentary cover of the

Drina–Ivanjica unit. Recent investigations have pointed out,

that the different carbonate blocks in the study area derive

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from a provenance area far to the east from the Drina–Ivanjica

unit (Missoni et al. 2012; Sudar et al. 2013; Gawlick et al.

2016 b). The overlying late Middle to early Late Jurassic

ophio

litic mélange (Gostilje–Ljubiš–Visoka–Radoševo

mélange: Gawlick et al. 2016b) is topped by the mafic and

ultramafic Dinaridic ophiolite nappes, which represent far

travelled ophiolite sheets from the Neo-Tethys, which was

located far to the east.

The studied ophiolitic mélange can be considered as

a sedimentary trench-like basin fill (sedimentary mélange).

The ophio litic mélange overlies the carbonate-clastic basin fill

of the Sirogojno mélange (Missoni et al. 2012; Sudar et al.

2013) and beside numerous different components from the

ophiolite suite it contains several radiolarite components from

the original sedimentary cover of the ocean floor.

Sampled sites, material and methods

Beside a lot of outcrops of the ophiolitic mélange south of

the study area the outcrops between Rožanstvo and Trnava

near Ilidža (Fig. 2) provide the rather rare possibility to study

components from the ophiolitic mélange which occur in

fissures of underlying limestone blocks (Fig. 3), fill depres-

sions between different limestone blocks or lie directly on top

of limestone blocks. Different components of the ophiolite

suite dominate the component spectrum. Radiolarite compo-

nents occur more rarely. The matrix consists of fine- and

coarse-grained sand made of eroded ophiolitic and radiolaritic

material.

We studied more than 10 different radiolarite pebbles of

different colours (greenish, reddish, red, violet) for the micro-

facies characteristics and the biostratigraphic age. Six radio-

larian samples yielded determinable and moderately preserved

radiolarian assemblages.

Results

Lithology and microfacies

Apart from the biostratigraphic age, microfacies analysis of

both radiolarites and limestones provides information about

their depositional setting (e.g., relative water depth, transport

regime, environment — e.g., bioturbating biota, oxygen con-

tent) and diagenetic overprint. Whereas microfacies analysis

of limestones is a common tool to describe their depositional

setting (Flügel 2004), microfacies analyses of radiolarites

remain rare, but, besides the overall lithofacies and the sedi-

mentation rate (Jenkyns & Winterer 1982; De Wever et al.

2001; Baum gartner 2013), they provide a powerful tool for the

reconstruction of the depositional realm of radiolaritic

sequences (Gawlick & Missoni 2015; Gawlick et al. 2016 a).

In certain cases the micro facies of the radiolarites is typical of

an age range. Microfacies differences not only reflect the

relative water depth (deposition on shelf areas versus

Fig. 3. Occurrence of the ophiolitic mélange in fissures of the

back-reef to lagoonal Dachstein Limestone between Trnava and

Rožanstvo. a — Microfacies of some clasts of the fine-grained

ophiolitic mélange which occurs in the fissures. Beside different

volcanic clasts also clasts of dark red radiolarites with recrystallized

radiolarians occur. Scale bar = 1 mm. b — Fine-grained ophiolitic

mélange consisting of volcanite grains and radiolarite grains in a glass

matrix. Scale bar = 1 mm. c — Field view of the fissures in the

Dachstein Limestone filled with coarse-grained ophiolitic mélange.

Violet-reddish and reddish radiolarite clasts beside the dark volcanic

clasts are well visible.

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depo sition on oceanic crust), the sizes of the radiolarians and

accompanying organisms (filaments, shells) also differ in rela-

tion to their age (Fig. 4).

Practically all radiolarite components from the ophiolitic

mélange between Trnava and Rožanstvo are violet-greyish,

violet-reddish or red, in some cases manganese-rich, as typical

for condensed oceanic ribbon radiolarites (e.g., Baumgartner

2013). They are completely bioturbated and therefore mas-

sive, in some cases mud-rich. All radiolarite components show

a more or less similar microfacies. Carbonate free radiolarian

wackestones to packstones in a muddy, in some cases com-

pletely silicified matrix are dominant. Filaments or crinoids,

as typical for shelf or continental slope near radiolarites are

completely missing in these radiolarite components (Gawlick

et al. 2016 a), they do not even occur as silicified ghosts. This

microfacies resembles oceanic radiolarites as described by

Gawlick et al. (2008, 2016 a, b).

Radiolarian dating

All samples with identifiable radiolarians derive from

the ophiolitic mélange on top of different carbonate blocks

fissure fillings. Samples SCG 48a and 48b derive

from the ophiolitic mélange overlying a Late Triassic

fore-reef to reefal block (reefal Dachstein Limestone).

Samples SCG 50, 51 and 52 derive from the ophiolitic

mélange filling a depression between the Late Triassic

fore-reef to reefal block and an Early Carnian reefal

limestone block (Wetterstein Formation). Sample

SRB 207 derives from a fissure infilling in Late Triassic

lagoonal to back-reef limestone (lagoonal Dachstein

Limestone).

The preservation of all radiolarians is rather poor, some-

times poor to moderate. In some cases they can be determined

only on the family level.

Fig. 4. Microfacies of the Late Triassic radiolarite components in the ophiolitic mélange near Ilidža on top of the carbonate-clastic mélange.

a — Bioturbated reddish-grey radiolarian packstone. Sample SCG 50, Scale bar = 1 mm. b — Enlargement of 1. The radiolarians are recrystal-

lized and occur as microquartz. The matrix is not completely slicified, in places the muddy matrix is still preserved and therefore the preserva-

tion of the radiolarians is moderate. Scale bar = 1 mm. c — Bioturbated violet-greyish radiolarian wackestone to packstone in a muddy and only

slightly slicified matrix. All radiolarians are preserved as microquartz. Sample SCG 51, Scale bar = 1 mm. d — Completely slicified greyish

radiolarite. The radiolarians occur as microquartz and are visible only as ghosts in the thin section. The preservation of the radiolarians is still

rather good. Sample SCG 52, Scale bar = 1 mm.

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Samples SCG 48a and b

Small reddish-grey radiolarite components from the ophio-

litic mélange on top of a Late Triassic fore-reef to reefal block.

Samples SCG 48a and SCG 48b are characterized by presence

of two distinctive assemblages:

SCG 48a (Fig. 5): Canesium sp., Capnodoce sp. cf. C. ana-

petes De Wever, C. sp. cf. C. extenta Blome, C. sp. cf. C. crys-

tallina Pessagno, C. sp. cf. C. sarisa De Wever, Capnucho sphaera

sp. cf. C. triassica De Wever, Corum sp. cf. C. speciosum

Blome, Japonocampe sp. cf. J. mundum (Blome), Spinosicapsa

sp., Praeprotunuma antiqua Tekin, Triassoastrum sp. cf.

T. noricum (Kozur & Mock). Taxa of this assemblage are com-

mon from the Upper Carnian to Lower Norian and probably

Middle Norian and are present in numerous localities of the

Mediterranean, western North America, Japan and Far Eastern

Russia (De Wever et al. 1979; Nakaseko & Nishimura 1979;

Pessagno et al. 1979; Blome 1983, 1984; Bragin 1991, 2007;

Sugiyama 1997; Tekin 1999). Due to relatively poor preserva-

tion the majority of taxa were determined in open nomencla-

ture, and the age should be determined in the broad interval

— from Upper Carnian to Middle Norian.

Sample SCG 48b (Fig. 5): Betraccium sp. aff. B. inornatum

Blome, Cantalum sp., Ferresium sp., Pantanellium sp.,

Tetraporobrachia sp. cf. T. composita Carter. This assemblage

is younger. Betraccium inornatum Blome is known from the

Upper Norian of Oregon (Blome 1983), from the Rhaetian of

Turkey (Tekin 1999), and from the Upper Norian of the New

Siberian Islands (Russia, Arctic) (Bragin 2011), while

Tetraporobrachia composita Carter was reported from the

Rhaetian of British Columbia (Carter 1993) and from the

Upper Norian of Turkey (Bragin & Tekin 1996) and Greece

Fig. 5. Late Triassic radiolarians from radiolarite components from the ophiolitic mélange on top of a Late Triassic fore-reef to reefal block.

1–14 — Radiolarians from sample SCG 48a (late Carnian to middle Norian): 1–2 — Capnuchosphaera sp. cf. C. triassica De Wever;

3 — Capnodoce sp. cf. C. sarisa De Wever; 4 — Capnodoce sp. cf. C. anapetes De Wever; 5 — Capnodoce sp. cf. C. crystallina Pessagno;

6 — Capnodoce sp. cf. C. extenta Blome; 7 — Triassoastrum sp. cf. T. noricum (Kozur & Mock); 8 — Praeprotunuma antiqua Tekin;

9 — Canesium? sp.; 10 — Canesium sp.; 11–12 — Japonocampe sp. cf. J. mundum (Blome); 13 — Corum sp. cf. C. speciosum Blome;

14 — Spinosicapsa sp.; 15–20 — Radiolarians from sample SCG 48b (late Norian–Rhaetian): 15 — Pantanellium sp.; 16–17 — Betraccium

sp. aff. B. inornatum Blome; 18 — Ferresium sp.; 19 — Cantalum sp.; 20 — Tetraporobrachia sp. cf. T. composita Carter.

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(Bragin et al. 2014). Therefore this assemblage can be dated as

Upper Norian–Rhaetian.

Sample SCG 50

Reddish Mn-rich massive radiolarite (Fig. 4) from a depres-

sion-fill between a Late Triassic fore-reef to reefal block

(Dachstein Limestone) and an Early Carnian reefal block.

The microfacies shows a bioturbated radiolarian packstone.

Other organisms are missing. The following taxa were deter-

mined (Fig. 6): Canesium sp., Canoptum? sp., Capnodoce

anapetes De Wever, C. crystallina Pessagno group, Capnucho-

sphaera sp., Corum regium Blome, C. sp. cf. C. regium Blome,

C. sp. cf. C. speciosum Blome, Crucella tenuis Tekin, Japono-

campe sp. aff. J. longulum (Blome), J. sp. cf. J. mundum

(Blome), Monocapnuchosphaera sp., Pachus sp., Poulpus sp. cf.

Fig. 6. Late Triassic (latest Carnian to early Norian) radiolarians from sample SCG 50. 1–2 — Tubospongopallium sp.; 3 — Triassoastrum sp.;

4 — Monocapnuchosphaera sp.; 5 — Capnuchosphaera sp.; 6–7 — Capnodoce crystallina Pessagno group; 8 — Capnodoce sp. cf.

C. crystallina Pessagno; 9 — Capnodoce anapetes De Wever; 10 — Poulpus sp. cf. P. piabyx De Wever; 11 — Crucella tenuis Tekin;

12 — Praeprotunuma antiqua Tekin; 13 — Praeprotunuma sp. cf. P. antiqua Tekin; 14 — Canesium sp.; 15 — Canoptum? sp.; 16 — Pachus

sp.; 17 — Corum regium Blome; 18 — Corum sp. cf. C. regium Blome; 19 — Corum sp. cf. C. speciosum Blome; 20 — Japonocampe sp. aff.

J. longulum (Blome); 21 — Japonocampe sp. cf. J. mundum (Blome); 22 — Spinosicapsa extansa (Tekin); 23 — Spinosicapsa sp. cf.

S. turgida (Blome); 24–25 —Spinosicapsa sp.

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P. piabyx De Wever, Praeprotunuma antiqua Tekin, Tubo-

spongopallium sp., Spinosicapsa extansa (Tekin), S. sp. cf.

S. turgida (Blome), S. sp., Triassoastrum sp. Tekin (1999)

restricted the stratigraphic interval of Crucella tenuis,

Praeprotunuma antiqua, and Spinosicapsa extansa to uppermost

Carnian–Lower Norian. Considering this conclusion, the age of

this sample ranges between the latest Carnian and Early Norian.

Sample SCG 51

Violet-reddish massive radiolarite with some mud lenses

(Fig. 4) from a depression-fill between a Late Triassic fore-

reef to reefal block (Dachstein Limestone) and an Early

Carnian reefal block (Wetterstein Limestone). The micro facies

shows a radiolarian wacke- to packstone with red mud

Fig. 7. Late Triassic radiolarians from radiolarite components from the ophiolitic mélange. 1–19 — Radiolarians from sample SCG 51 (latest

Carnian to early Norian): 1–2 — Xiphothecaella sp. cf. X. longa (Kozur & Mock); 3 — Triassoastrum? sp.; 4 — Capnuchosphaera theloides

De Wever; 5 — Capnuchosphaera sp. cf. C. triassica De Wever; 6 — Capnuchosphaera sp.; 7–8 — Capnodoce crystallina Pessagno group;

9 — Poulpus sp. cf. P. piabyx De Wever; 10 — Praeprotunuma sp. cf. P. antiqua Tekin; 11 — Spinosicapsa sp. cf. S. yazgani (Tekin);

12 — Pachus sp. cf. P. multinodosus Tekin; 13 — Pachus sp. cf. P. firmus Blome; 14 — Xipha sp. cf. X. pessagnoi (Nakaseko & Nishimura);

15 — Corum speciosum Blome; 16 — Corum sp. cf. C. speciosum Blome; 17 — Corum sp. cf. C. regium Blome; 18 — Canoptum sp. cf.

C. macoyense Blome; 19 — Spinosicapsa sp. cf. S. turgida (Blome). 20–22 — Radiolarians from sample SCG 52 (Carnian to middle Norian):

20 — Saturnalidae gen. indet; 21 — Corum sp. cf. C. speciosum Blome; 22 — Japonocampe sp. cf. J. mundum (Blome).

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lenses. The following taxa were determined (Fig. 7): Canoptum

sp. cf. C. macoyense Blome, C. crystallina Pessagno group,

Capnuchosphaera theloides De Wever, C. sp. cf. C. triassica

De Wever, Capnuchosphaera sp., Corum sp. cf. C. regium

Blome, C. speciosum Blome, Crucella? sp., Xipha sp. cf.

X. pessagnoi (Nakaseko & Nishimura), Pachus sp. cf.

P. firmus Blome, P. sp. cf. P. multinodosus Tekin, Poulpus sp.

cf. P. piabyx De Wever, Praeprotunuma sp. cf. P. antiqua

Tekin, Spinosicapsa

sp. cf. S. yazgani (Tekin), Spinosicapsa

sp. cf. S. turgida (Blome), Triassoastrum? sp., Xiphothecaella

sp. cf. X. longa (Kozur & Mock). This assemblage is very

similar to SCG 50 and has a similar age: Uppermost Carnian–

Lower Norian.

Sample SCG 52

Greyish-greenish massive radiolarite (Fig. 4) from a depres-

sion-fill between a Late Triassic fore-reef to reefal block

(Dachstein Limestone) and an Early Carnian reefal block

(Wetterstein Limestone). The original microfacies of this

radio larite is masked by the intense silicification, radiolarians

are only visible as ghosts. Due to poor preservation only a few

specimens were determined (Fig. 7): Canesium? sp., Canoptum

sp., Capnodoce? sp., Corum sp. cf. C. speciosum Blome,

Crucella sp., Japonocampe sp. cf. J. mundum (Blome),

Tubospongopallium sp., Saturnalidae gen. indet.,

Triassoastrum? sp. The age of the sample is Upper Triassic,

Carnian to Middle Norian according to the presence of

Corum sp. cf. C. speciosum Blome and Japonocampe sp. cf.

J. mundum (Blome).

Sample SRB 207

Reddish-violet muddy radiolarite from a fissure fill consis-

ting of ophiolitic mélange in lagoonal to back-reef Late

Triassic Dachstein Limestone. The following taxa were deter-

mined (Fig. 8): Braginella sp. cf. B. rudis (Bragin), Cantalum?

sp., Ferresium sp. cf. F. triquetrum Carter, Ferresium sp.,

Sarla? sp., Saturnalidae gen. indet., Serilla sp. cf. S. ellisensis

(Carter). Ferresium triquetrum is present in the Rhaetian of

British Columbia (Carter 1993) and from the Upper Norian of

Turkey (Bragin & Tekin 1996). Serilla ellisensis is known

from the Rhaetian of British Columbia (Carter 1993), while

Braginella rudis was reported from the Upper Norian of Far

East Russia (Bragin 1991), Japan (Sugiyama 1997) and Greece

(Bragin et al. 2014). The age of this radiolarian assemblage is

Upper Norian–Rhaetian.

Sedimentology

The ophiolitic mélange overlies different Triassic carbonate

blocks filling the rough topography of an older carbonate-

clastic basin fill (Fig. 9; Sirogojno carbonate-clastic mélange:

Missoni et al. 2012; Sudar et al. 2013). Coarse-grained turbi-

dites and mass transport deposits beside fine-grained radio-

laritic-argillaceous sediments and turbidites consisting of

ophiolitic sand and radiolarites (Fig. 3) are the dominant sedi-

mentary rocks and occur in fissures of the underlying carbo-

nate rocks (Fig. 3) or fill the depressions between huge

slide blocks. The sedimentological features document clearly

a sedi mentary rather than a tectonic genesis of the ophiolitic

mélange west of the Drina–Ivanjica unit. Fine-grained turbi-

dites consisting of ophiolitic sand occur beside coarse-grained

mass transport deposits and m-sized blocks. Matrix radiola rites

are missing in this lowermost part of the ophiolitic mélange.

In this early stage of erosion and redeposition of the ophio-

litic nappe stack only Upper Triassic radiolarites occur beside

ophiolite components. Higher up in the mélange we also find

Middle Triassic radiolarites and radiolarite/limestone com-

ponents/blocks from the continental slope as described by

Fig. 8. Late Triassic (late Norian–Rhaetian) radiolarians from radiolarite from sample SRB 207. 1–2 — Ferresium? sp.; 3 — Ferresium sp. cf.

F. triquetrum Carter; 4–5 — Sarla? sp.; 6 — Cantalum? sp.; 7 — Serilla sp. cf. S. ellisensis (Carter); 8 — Braginella sp. cf. B. rudis (Bragin).

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, 2017, 68, 4, 350 – 365

Gawlick et al. (2016 b). This clearly indicates 1) deeper ero-

sion of the sedimentary cover on top of the oceanic crust (Late

Anisian to Jurassic) including the tectonic incorporation of

blocks from the continental slope in the course of westward

obduction or 2) erosion of the sedimentary cover of ophiolites

in a higher nappe position (Fig. 10 b, c), a more convincing

possibility (Fig. 9; see also discussion). Therefore we assign

the ophiolitic mélange in the eastern part of the Dinaridic

Ophiolite Belt originally to be a sedimentary mélange, depo-

sited in a trench-like basin in front of the westward propa-

gating ophiolite sheets.

Discussion

Although there are contrasting models about the palaeo-

geography in Triassic–Jurassic times in the western Tethyan

realm (e.g., Stampfli & Kozur 2006; Schmid et al. 2008;

Missoni & Gawlick 2011b; Robertson 2012; Gawlick et al.

2016 a, b), there is progress in the reconstruction of the age of

lost oceanic domains and in the understanding of geodynamic

processes in the Tethyan realm. Many new biostratigraphic

data on Triassic and Jurassic radiolarites in mélange areas

have recently been obtained in the Dinarides, Albanides and

Hellenides (e.g., Gawlick et al. 2008, 2016 a, b; Vishnevskaya

et al. 2009; Djerić et al. 2010, 2012; Chiari et al. 2011, 2013;

Ozsvárt et al. 2012; Bragin et al. 2014; Ferrière et al. 2015,

2016; Gawlick & Missoni 2015), but still a lot of questions

remain open. Detailed microfacies investigations and biostra-

tigraphic data allow detailed information about the deposi-

tional history for both the carbonate (e.g., Flügel 2004) and the

radiolarite sequences. Such combined investigations on radio-

larites remain rare (e.g., Gawlick et al. 2009 a, 2016 a, b;

Krische et al. 2014; Gawlick & Missoni 2015), but the recon-

struction of the depositional environment of radiolarites pro-

vides a number of answers for the open questions.

The investigations of the resedimented Late Triassic oceanic

ribbon radiolarite clasts in the ophiolitic mélange between

Trnava and Rožanstvo result in a reconstruction of their pri-

mary depositional realm and give further evidence on the

Triassic–Jurassic geodynamic history as well as on the palaeo-

geographic evolution of the Inner Dinarides, especially the

Dinaridic Ophiolite Belt.

Blocks from the Neo-Tethys ocean floor with the preserved

sedimentary cover occur rarely in the different mélanges of the

Dinaridic Ophiolite Belt. One Late Ladinian (to Carnian)

basalt-radiolarite block was described by (Vishnevskaya et al.

2009), probably another one by Gawlick et al. (2016b) whereas

younger ocean floor blocks were not detected. Descriptions of

Upper Triassic ribbon radiolarites from the ocean floor also

remain rare (Obradović & Goričan 1988; Goričan et al. 1999;

Gawlick et al. 2009 b, 2016 b; Vishnevskaya et al. 2009).

Middle Triassic radiolarite blocks are more common (summa-

rized in Chiari et al. 2011).

There is a controversy about the genesis of the ophiolitic

mélange: A) Tectonic origin with incorporation of blocks from

Fig. 9. The ophiolitic mélange on top of the carbonate-clastic mélange below filling depressions and fissures. a — Field situation: a huge

limestone block covered by the ophiolitic mélange. The limestone block is more stable against weathering and therefore forms positive relief.

b — Reconstruction of the depositional realm, provenance area of the ophiolitic mélange (Neo-Tethys ophiolite nappe stack) and sample

positions. c — Ophiolitic mélange as fissure filling in lagoonal Dachstein Limestone.

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the overridden plate, B) Sedimentary origin (olistostrome), or

C) original sedimentary trench-fill later incorporated in the

nappe stack. The area where the ophiolitic mélange of the

Dinaridic Ophiolite Belt was formed is completely unclear.

Several hypotheses exist: 1) Formation of the ophiolitic

mélange either in the framework of intra-oceanic subduction,

or 2) on the base of ophiolite sheets when obduction starts

with incorporation of blocks from the overridden lower plate.

Gawlick et al. (2016 b) showed, that the ophiolite mélange of

the Dinaridic Ophiolite Belt was first formed as sedimentary

trench-fill later incorporated in the nappe stack. But the

question of where the ophiolitic mélange was formed remains

unclear. Solution of this geographical question is important for

the still controversial discussed problem: Do the ophiolites

including the ophiolitic mélange of the Dinaridic Ophiolite

Belt represent far-travelled and obducted ophiolites from the

Neo-Tethys to the east (e.g., Gawlick et al. 2008, 2009 b,

2016 b; Schmid et al. 2008) or are they relics of an auto-

chthonous oceanic realm between the Durmitor mega-unit

to the west and the Drina–Ivanjica unit to the east (e.g.,

Dimitrijević 1997; Karamata 2006)? For a recent review on

this problem see Gawlick et al. (2016 b). In addition, it is

believed that the different carbonate blocks in the area

west of Sirogojno derive from the Drina–Ivanjica unit

directly to the east (e.g., Dimitrijević & Dimitrijević 1973,

Dimitrijević 1997). Missoni et al. (2012) and Sudar et al.

(2013) showed that the different blocks of the carbonate-

clastic Sirogojno Mélange (Sudar et al. 2013) derive from

a provenance area east of the Drina–Ivanjica unit (Fig. 10 a).

The studied ophiolitic mélange between Trnava and

Rožanstvo filled the depression of an older trench-like basin

fill with a rough topography (Fig. 9). In the first phase of depo-

sition the turbidites and mass-flow deposits filled the fissures

and depression of the older topography. It is important is to

note, that the underlying blocks derive exclusively from the

Late Triassic back- to fore-reef facies belt (Fig. 10). Therefore

this ophiolitic mélange on top of the carbonate-clastic

Sirogojno Mélange was transported later to its recent position

west of the Drina–Ivanjica unit. The Late Triassic sedimentary

succession of the Drina–Ivanjica unit comprises lagoonal

Dachstein Limestones (Dimitrijević & Dimitrijević 1991;

Dimitrijević 1997).

The ophiolitic mélange is, according to recent descriptions

and definitions (summarized in Chiari et al. 2011; Gawlick et

al. 2016 a) a typical sub-ophiolitic mélange and consists of

a mixture of blocks and slices of the oceanic domain (e.g.,

oceanic rocks: ultramafic rocks, gabbroic and basaltic rocks;

oceanic sediments: ophicalcites, radiolarites, deep-sea muds;

amphibolites) and the obducted former distal passive margin,

namely the continental slope (Meliata facies: Fig. 10a). These

blocks are incorporated in a sedimentary matrix, very often

turbiditic argillaceous-radiolaritic sediments and coarser-

grained sands, consisting of erosional products of the ophiolite

nappe stack. Such a mélange can incorporate fragments of the

underlying sequences during the process of overthrusting.

Therefore, such a sub-ophiolite mélange contains blocks from

the lower plate and gravitationally emplaced blocks derived

from the thick wedge of oceanic and continental crust at the

front of the advancing nappe pile. In addition, as described by

Gawlick et al. (2008) and Missoni & Gawlick (2011a) trench-

like basins were formed in front of the advancing nappes.

These deep-water basins were supplied by the erosional pro-

ducts of the advancing nappe stack. Several types of mass

transport deposits (for a review on Mass Transport Deposits

see: Shanmugam 2015) are incorporated in such a turbiditic

radiolaritic-argillaceous matrix. Later, these trench-like basins

were incorporated in the nappe stack and became partly

sheared, forming the typical features of a mélange.

During ongoing westward directed ophiolite obduction and

imbrication of the older (Triassic–Middle Jurassic) sedimen-

tary succession of the former passive continental margin

facing the Neo-Tethys Ocean to the east (Fig. 10a), now in

a lower plate position, a series of trench-like basins were

formed in front of the propagating nappe stack (Fig. 10 b, c).

The first basin formed in the course of ophiolite obduction

contains material from the ophiolite nappe stack and the con-

tinental slope (Meliata facies belt, Fig. 10 a), later incorporated

into the nappe stack. Imbrication of the former passive margin

led to the formation of a series of such trench-like basins of the

westward propagating nappe stack (Fig. 10 b, c). In the next

phase, the former distal passive margin became incorporated

into the nappe stack (Hallstatt facies belt with the various

coloured Hallstatt Limestones: Lein 1987; Sudar et al. 2010).

In a later stage the facies belts of the reef-near open marine

facies belt and the fore-reef to back-reef facies belt became

imbricated. These basins formed in front of the propagating

nappe stack contain in the first stage of redeposition only

resedimented material from the adjacent nappe front, as

described in detail for the Northern Calcareous Alps by

Gawlick et al. (1999, 2012 b) and Missoni & Gawlick

(2011a, b). All these basin fills are characterized by a coarse-

ning-upward cycle with huge slide blocks on top of the basin

fill, which may in some cases also represent remnants of the

overriding nappe (Gawlick et al. 2012 b). A little later, ongoing

westward directed ophiolite obduction also affected these

basin fills: Redeposition of material derived from the advan-

cing ophiolite nappe stack in the area where the Sirogojno

carbonate-clastic mélange was formed filled in the first stage

of deposition the remaining topography of the older basin fill

(Figs. 9, 10 c), but still in an area east of the Drina–Ivanjica unit.

The final emplacement of the ophiolites and the mélanges

west of the Drina–Ivanjica unit (Fig. 10 d), namely in the area

of the Dinaridic Ophiolite Belt occurred later, most probably

in the latest Jurassic or earliest Cretaceous in the course of

ongoing westward transport of the ophiolites and the mélanges

(Schmid et al. 2008; Djerić et al. 2012).

Conclusions

Late Triassic radiolarites are of special interest for the

reconstruction of the Jurassic geodynamic history of the

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, 2017, 68, 4, 350 – 365

Neo-Tethys oceanic domain, because they indicate fragments

of the Neo-Tethys oceanic realm. The Late Triassic radiolarite

components in the ophiolitic mélange on top of the carbonate-

clastic mélange in the eastern part of the Dinaridic Ophiolite

Belt suggest the following conclusions:

• The ophiolitic mélange in the Dinaridic Ophiolite Belt is of

primary sedimentary origin.

• Deposition of the mass transport deposits of the ophiolitic

mélange took place in a deep-water trench-like basin formed

in the late Middle Jurassic east of the Drina–Ivanjica unit.

• The Late Triassic ribbon radiolarites represent erosional

products of the original sedimentary cover of the Middle

Triassic to Early Jurassic Neo-Tethys ocean floor.

• Older components like Middle Triassic radiolarites or com-

ponents from the distal continental margin are missing in the

early mass transport deposits. The components represent

erosional products of an ophiolite sheet from more distal

oceanic areas, which were in a relatively high nappe posi-

tion at that time.

• The ophiolites of the Dinaridic Ophiolite Belt including the

ophiolitic mélange derived as far-travelled oceanic sheets

from the Neo-Tethys Ocean to the east.

Acknowledgements: Thin sections were prepared by Per

Jeisecke (University of Tübingen). This research was suppor-

ted by Ministry of Education, Science and Technological

Development of the Republic of Serbia, Project ON-176015

(NDJ, MS, DJ). The cooperation Leoben-Belgrade was sup-

ported by the CEEPUS Network CIII-RO-0038 Earth-Science

Studies in Central and South-Eastern Europe. The research

work of N. Bragin was supported by Russian Governmental

Assignment no. 0135-2014-0064. The careful review of Špela

Goričan (Ljubljana) and the helpful suggestions of Roman

Aubrecht (Bratislava) are gratefully acknowledged.

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