GeolCarp_Vol61_No2_89

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA, APRIL 2010, 61, 2, 89—109 doi: 10.2478/v10096-010-0003-6

Introduction

Whereas the stratigraphy of the external zones of the Dinari-
des is relatively well known, the sedimentary and paleotec-
tonic  evolution  of  the  internal  zones  is  less  understood.  In
part  this  is  due  to  Alpine  metamorphic  overprint,  in  part  to
the structural complexities of the area. In particular, there ex-
ists an ongoing controversy about the original paleogeogra-
phy  and  how  many  basins  underlain  by  oceanic  lithosphere
existed in Mesozoic times between the Adriatic microconti-
nent, of which the external Dinarides are part, and Europe in-
cluding  smaller  continental  fragments  (Tisza,  Dacia)
detached from it. The case of a one-ocean model has been ar-
gued for by authors on different occasions (e.g. Bernoulli &

Triassic metasediments in the internal Dinarides (Kopaonik

area, southern Serbia): stratigraphy, paleogeographic and

tectonic significance

SENECIO SCHEFER

, DANIEL EGLI

1,2

, SIGRID MISSONI

, DANIEL BERNOULLI

1,2

BERNHARD FÜGENSCHUH

, HANS-JÜRGEN GAWLICK

, DIVNA JOVANOVIĆ

LEOPOLD KRYSTYN

, RICHARD LEIN

, STEFAN M. SCHMID

1,8

and MILAN N. SUDAR

University of Basel, Institute of Geology and Paleontology, Bernoullistrasse 32, 4056 Basel, Switzerland;

senecio.schefer@unibas.ch; daniel.bernoulli@unibas.ch; stefan.schmid@unibas.ch

ETH Zürich, Geological Institute, Sonneggstr. 5, 8092 Zürich, Switzerland; daniel.egli@erdw.ethz.ch

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

8700 Leoben, Austria; hans-juergen.gawlick@mu-leoben.at; s.missoni@daad-alumni.de

University of Innsbruck, Institute of Geology and Paleontology, Innrain 52, 6020 Innsbruck, Austria; bernhard.fuegenschuh@uibk.ac.at

Geological Institute of Serbia, Rovinjska St. 12, 11000 Belgrade, Serbia; djdivna@gmail.com

University of Vienna, Department of Paleontology, Althanstrasse 14, 1090 Vienna, Austria; leopold.krystyn@univie.ac.at

University of Vienna, Centre for Earth Sciences, Althanstrasse 14, 1090 Vienna, Austria; richard.lein@univie.ac.at

now at FU Berlin, Institut für Geologische Wissenschaften, Malteserstrasse 74—100, D-12249 Berlin, Germany

University of Belgrade, Faculty of Mining and Geology, Department of Paleontology, Kamenička St. 6, P.O. Box 227, 11000 Belgrade,

Serbia; sudar@eunet.rs

(Manuscript received June 1, 2009; accepted in revised form October 2, 2009)

Abstract: Strongly deformed and metamorphosed sediments in the Studenica Valley and Kopaonik area in southern
Serbia expose the easternmost occurrences of Triassic sediments in the Dinarides. In these areas, Upper Paleozoic
terrigenous sediments are overlain by Lower Triassic siliciclastics and limestones and by Anisian shallow-water car-
bonates. A pronounced facies change to hemipelagic and distal turbiditic, cherty metalimestones (Kopaonik Formation)
testifies a Late Anisian drowning of the former shallow-water carbonate shelf. Sedimentation of the Kopaonik Forma-
tion was contemporaneous with shallow-water carbonate production on nearby carbonate platforms that were the source
areas of diluted turbidity currents reaching the depositional area of this formation. The Kopaonik Formation was dated
by conodont faunas as Late Anisian to Norian and possibly extends into the Early Jurassic. It is therefore considered an
equivalent of the grey Hallstatt facies of the Eastern Alps, the Western Carpathians, and the Albanides—Hellenides. The
coeval carbonate platforms were generally situated in more proximal areas of the Adriatic margin, whereas the distal
margin was dominated by hemipelagic/pelagic and distal turbiditic sedimentation, facing the evolving Neotethys Ocean
to the east. A similar arrangement of Triassic facies belts can be recognized all along the evolving Meliata-Maliac-
Vardar branch of Neotethys, which is in line with a ‘one-ocean-hypothesis’ for the Dinarides: all the ophiolites pres-
ently located southwest of the Drina-Ivanjica and Kopaonik thrust sheets are derived from an area to the east, and the
Drina-Ivanjica and Kopaonik units emerge in tectonic windows from below this ophiolite nappe. On the base of the
Triassic facies distribution we see neither argument for an independent Dinaridic Ocean nor evidence for isolated
terranes or blocks.

Key words: Triassic, Dinarides, Kopaonik, Serbia, stratigraphy, conodonts.

Laubscher  1972;  Gawlick  et  al.  2008;  Schmid  et  al.  2008)
and  will  not  be  discussed  in  detail  here.  In  brief,  the  one-
ocean model according to Schmid et al. (2008) proposes that
(a) all the Jurassic-age ophiolites of the Dinarides, including
their  supra-subduction  magmatic  rocks,  originate  from  one
and the same ocean and (b) this ocean also included Triassic-
age  oceanic  crust  bordering  the  Mesozoic  Adriatic  margin,
from which only fragments referred to as Meliata in Slovakia
and Maliac in Greece are preserved. Consequently, we shall
call this oceanic branch of the Neotethys the Meliata-Maliac-
Vardar  Ocean.  In  contrast  to  our  one-ocean  model,  Robert-
son  &  Karamata  (1994),  Dimitrijević  (1997,  2001)  and
Karamata (2006) envisage at least two different oceanic ba-
sins  floored  by  Jurassic  oceanic  crust  originally  separated

SCHEFER et al.

from  each  other  by  intervening  ‘terranes’  of  continental
crust, the Drina-Ivanjica, Jadar and Kopaonik ‘terranes’ (see
Robertson  et  al.  2009  for  discussion).  In  our  interpretation,
however, these ‘terranes’ are tectonic windows of the distal
Adriatic  margin  below  an  ophiolite  nappe  referred  to  as
Western Vardar Ophiolitic Unit, obducted in the Late Juras-
sic  (Schlagintweit  et  al.  2008;  Schmid  et  al.  2008)  and  in-
cluding all ophiolites of the Dinarides west of the Sava Zone
(Fig. 1;  Western  Vardar  Ophiolites).  In  addition,  our  one-
ocean  model  is  in  contrast  to  earlier  models  that  attributed
the remnants of Triassic-age oceanic crust found within Ju-
rassic  mélanges  in  Slovakia  (Meliata;  Channell  &  Kozur
1997), within Jurassic mélanges tectonically underlying ob-
ducted Jurassic ophiolites in the Dinarides (Vishnevskaya et
al.  2009)  or  as  tectonic  imbricates  below  obducted  Jurassic
ophiolites in Greece (Maliac; Ferri

re 1982) to other separate

oceanic basins (e.g.  Stampfli  &  Borel  2004).  The  basement
complexes  of  the  Drina-Ivanjica  and  the  Jadar-Kopaonik
thrust  sheets  including  their  formerly  emplaced  allochtho-
nous  ophiolitic  cover  have  been  involved  in  further  out-of-
sequence  and  frontal  thrusting  onto  the  more  external  East
Bosnian-Durmitor  thrust  sheet  during  the  Late  Cretaceous
(Rampnoux 1970, 1974; Schmid et al. 2008).

The reconstruction of the Triassic-Jurassic paleogeogra-

phy  of  the  Dinarides,  which  involves  the  reconstruction  of
the facies belts of the Triassic shallow-water carbonate plat-
forms  and  their  transition  to  the  hemipelagic  and  pelagic
(‘Hallstatt’) facies belt, play an important role for the various
tectonic  concepts  and  paleogeographic  reconstructions.  In  a
one-ocean model, we would expect a single continental-mar-
gin wedge of marine sediments with a general proximal-to-
distal  transition  from  shallow-  to  deep-water,  facing  the
Triassic  to  Jurassic  Meliata-Maliac-Vardar  Ocean  (or  Neo-
tethys)  to  the  east.  In  contrast,  according  to  various  more-

than-one ocean models, we would expect isolated fragments
of shallow- or deep-water deposits with differing facies evo-
lutions.  In  this  contribution,  we  attempt  to  characterize  the
Mesozoic  sedimentary  evolution  of  an  internal  part  of  the
Drina-Ivanjica thrust sheet (‘Studenica slice’ of Dimitrijević
1997)  and  of  the  Jadar-Kopaonik  thrust  sheet  near  Ušće  in
western Serbia (Fig. 2), which expose the easternmost occur-
rences of Triassic sediments in the Dinarides in windows be-
low the ophiolites (Grubić et al. 1995: their fig. 1).

Geological setting and metamorphism

The study area includes a metamorphic part of the internal

Drina-Ivanjica  thrust  sheet  (‘Studenica  slice’)  and  the  low-
grade  metamorphic  Kopaonik  thrust  sheet.  Both  carry  their
previously emplaced allochthonous ophiolite covers (Fig. 2)
(Schmid et al. 2008). These two units have been considered
to be part of the Vardar Zone as originally defined by Koss-
mat  (1924)  also  including  the  successions  underlying  the
ophiolites (e.g. Rampnoux 1974; Charvet 1978; Dimitrijević
1997,  2001).  However,  the  co-occurrence  of  oceanic  and
continental  basement  rocks  precludes  such  a  simple  defini-
tion and is unfortunate because the term ‘Vardar’ is usually
associated  with  ophiolites.  In  our  interpretation,  both  the
Studenica  slice  and  Jadar-Kopaonik  thrust  sheet  are  part  of
the  distal  Adriatic  margin,  covered  by  the  obducted  Upper
Jurassic ophiolite nappe. The Studenica Metamorphic Series
and the Kopaonik Metamorphic Series (Egli 2008; Schefer et
al. 2008) of the internal Drina-Ivanjica and the Jadar-Kopa-
onik  thrust  sheet,  respectively  (Fig. 2),  include  a  Paleozoic
metasedimentary basement, overlain by metamorphic Trias-
sic  to  Middle/?Upper  Jurassic  sediments.  The  Studenica
Metamorphic  Series  and  the  Kopaonik  Metamorphic  Series

Fig. 1. Tectonic map of the southern Dinarides, modified after
Schmid et al. (2008).

Fig. 2. Tectonic map of the Kopaonik area, based on mapping by S. Schefer and D. Egli and on the Basic Geological Map of the SFRY
(1:100,000), Sheets Novi Pazar (Urošević et al. 1970a, 1973a), Vrnjci (Urošević et al. 1970b, 1973b), Sjenica (Mojsilović et al. 1978, 1980)
and Ivanjica (Brković et al. 1976, 1977) as well as Simić (1956) for the Studenica area. Coordinates are in MGI Balkan 7.

SCHEFER et al.

have been thrust, together with their ophiolitic covers, as a
composite nappe onto the Drina-Ivanjica thrust sheet to the
west during the Late Cretaceous (Fig. 2).

The Mesozoic metasediments of the Kopaonik and

Studenica Metamorphic Series show a polyphase penetrative
tectonic  overprint  (Egli  2008),  associated  with  polyphase
Cretaceous and Paleogene greenschist-facies metamorphism
that  locally  reaches  lower-amphibolite  grade  conditions
(Schefer et al. 2008). This greenschist-facies metamorphism
is  also  reflected  by  the  thermal  alteration  of  conodonts,
which change their colour from yellow to light brown, then
to  dark  brown  and  black,  later  to  grey  and  finally  to  white.
This  conodont  colour  change  is  expressed  in  terms  of  the
Conodont Colour Alteration Index (CAI-values 1—8) that can
be related to certain temperature intervals ranging from less
than 80 °C to more than 600 °C (Epstein et al. 1977; Harris
1979; Rejebian et al. 1987). In addition, structural modifica-
tions  of  conodonts  also  provide  information  on  contact-
metamorphic/hydrothermal  events  (Epstein  et  al.  1977;
Rejebian  et  al.  1987;  Königshof  1992;  Burnett  et  al.  1994).
In part of our samples, conodonts with CAI 5.5—6.0 occur to-
gether  with  scarce  specimens  that  exhibit  CAI  values  of  up
to CAI 7.0. Such conodonts show a whitish patina and corro-
sion on their surface, in contrast to conodonts of CAI 5.5—6.0.
We interpret the higher CAI-values related to a contact meta-
morphic event overprinting the already deformed and meta-
morphosed rocks. This later event can be correlated with the
Oligocene intrusion of the Kopaonik granodiorite (Schefer et
al.  2008)  that  thermally  altered  the  surrounding  host  rocks
(Knežević et al. 1995).

According to Knežević et al. (1995), the contact-metamor-

phic rocks (skarn and hornfelses) around the Kopaonik grano-
diorite  record  P-T-conditions  of  565 °C  and  100 ± 50 MPa,
which is in line with CAI values of up to 7.0 (Epstein et al.
1977; Harris 1979) assuming a short time interval of heating
to more than 550 °C (Nöth 1991; Burnett et al. 1994) associ-
ated with hot-fluid circulation derived from the Kopaonik in-
trusion.  These  mixed  CAI  values  of  CAI 5.5  and
CAI 6.5—7.0  in  one  sample  can  only  be  explained  by  the
contact-metamorphic  overprint  by  the  Kopaonik  intrusion
while the lower CAI values of 5.5—6.0 record the earlier re-
gional  metamorphic  event  contemporaneous  with  the  main
deformation (Egli 2008).

Because of the metamorphic overprint, all metamorphic

sequences in the Kopaonik region and those developed west
of the Ibar Valley were often mapped as Paleozoic (Urošević
et al. 1970a,b, 1973a,b; Brković et al. 1976, 1977; Mojsilović
et al. 1978, 1980), although a Triassic-age of the carbonates
in  the  Studenica  area  was  postulated  much  earlier  (Simić
1956). Indeed, conodonts of Carnian age were discovered in
the metamorphic rocks of the Kopaonik area (‘Central Kopa-
onik  Series’  in  the  north:  Mićić  et  al.  1972;  ‘Metamorphic
Trepča Series’ in the south: Klisić et al. 1972). Sudar (1986)
confirmed  this  Carnian  age,  and  in  addition,  found  Norian
conodonts; he also established a biostratigraphic subdivision
of the cherty limestones into conodont zones. The metamor-
phosed and ductilely deformed conodonts (CAI values 5—7)
from Kopaonik Mountains were first described and illustrat-
ed by Sudar & Kovács (2006).

Location of sections

Studenica

This section (Fig. 3a) is located downstream from the

Studenica monastery (Fig. 2) near a bridge over the Studenica
River. After the Studenica quarry it follows the road for about
500 m downstream from the bridge. The northwestern base of
the  section  is  located  at  coordinates  7463300/4815000  (this
and all following localities are given in the MGI Balkan7 Car-
tesian  coordinates  also  used  for  the  1 : 100,000  geological
maps of former Yugoslavia). The highly deformed rocks were
recrystallized under greenschist-facies conditions and show a
strong  and  occasionally  mylonitic  foliation  and  NNW—SSE-
oriented  stretching  lineation.  This  resulted  in  a  considerably
reduced  thickness  of  the  sequence.  The  section  starts  with
massive  Anisian  dolostones  and  ends  in  the  ophiolitic  mé-
lange underlying the ophiolite nappe (Fig. 3a).

Gradac

The two sections near the village of Gradac are located fur-

ther  south  in  the  Studenica  unit,  west  of  the  Ibar  River
(Fig. 2). Both profiles, particularly section Gradac 2, show in-
tense deformation under greenschist-grade metamorphic con-
ditions.  Section  Gradac 1  starts  3 km  west  of  Gradac  village
and  stretches  along  the  road  to  Ivanjica  between  coordinates
7460710/4803253  and  7461274/4802826.  This  section  in-
cludes the succession from the upper part of the Lower Trias-
sic  Werfen  Formation  (probably  Campil  Beds)  to  Anisian
shallow-water carbonates. Section Gradac 2 is located north of
the hamlet Jokovići and along the road to Dolovi, between co-
ordinates  7460889/4806460  and  7461163/4806257.  It  also
starts with the Werfen Formation (probably Campil Beds) but
exposes the succession up to the siliceous metalimestones of
the  Kopaonik  Formation  (Fig. 3b);  however,  part  of  the  suc-
cession  is  cut  out  by  faults.  In  this  section,  the  rocks  are
strongly deformed, showing a distinct stretching lineation and
top-to-the-north shear-senses, whereas Gradac 1 is only slight-
ly deformed, showing minor stretching in a NW—SE direction
and open folding.

Kopaonik area

This area located east of the Ibar River and on the south-

eastern  slope  of  the  Kopaonik  Mountain  (NE  of  Pančićev
Vrh)  was  mapped  at  the  scale  1:10,000  by  Egli  (2008)
(Fig. 4).  The  oldest  rocks  are  quartz-phyllites  of  probably
Paleozoic  age,  overlain  by  the  Werfen  Formation  followed
up-section  by  shallow-water  carbonate  sediments  (‘Guten-
stein’ and ‘Steinalm’ equivalents). A vast amount of the out-
cropping  rocks,  however,  consists  of  well-bedded  cherty
metalimestones  of  the  newly  defined  Kopaonik  Formation
(see below). This stratigraphic succession underwent strong
polyphase  folding  under  greenschist-facies  conditions  (Egli
2008;  Zelić  et  al.  2010).  Near-isoclinal  D2-folds  dominate
the map pattern. In the vicinity of the Kopaonik granodioritic
intrusion  (30.7—30.9 Ma;  Schefer  et  al.  2008)  we  also  find
contact  metamorphic  rocks  (skarns  and  hornfelses).  Field

SCHEFER et al.

evidence shows that intrusion and contact metamorphism
postdate regional metamorphism and main deformation.

Stratigraphy

Quartz-phyllites

In the Kopaonik area, this formation is only preserved in

some  small  outcrops  bordering  the  Kopaonik  granodiorite
(Fig. 4).  Layers  of  pelitic  composition  are  interbedded  with
quartzitic layers. On weathered surfaces, the finely laminated
rocks  are  grey  to  reddish  in  colour,  but  grey  to  greenish  on
fresh surfaces. While a narrow-spaced bedding-parallel folia-
tion  develops  in  the  phyllitic  layers,  the  quartzitic  layers  are
often boudinaged. These rocks are probably of Paleozoic age
but,  alternatively,  they  may  represent  the  lowermost  part  of
the Lower Triassic Werfen Formation.

Werfen Formation

In the Kopaonik area, massive metasandstones, typical for

the lower part of the Werfen Formation, are visible in small
outcrops located close to the intrusion (Egli 2008). The sand-
stones  are  brownish  to  reddish  on  weathered  surfaces  and
dark brown to black on fresh surfaces. Detrital grains (usual-
ly  < 1  mm)  and  cement  are  entirely  made  up  of  quartz.  In
coarse-grained layers, cross-bedding (Fig. 5a) or a faint par-
allel  lamination,  as  well  as  a  bedding-parallel  foliation  can
be observed. In thin-section, small biotite flakes defining the
foliation are present besides quartz. In the vicinity of the in-
trusion, the rocks are overprinted by contact metamorphism,
which  leads  to  the  formation  of  white  mica,  garnet  and
brown amphiboles with grains between 0.1 and 1 mm (Egli
2008).

The upper part of the Werfen Formation shows similarities

with the basal part of the Gradac 1 and 2 successions and

Fig. 5. Lower and Middle Triassic lithofacies. a – Cross-bedded sandstone, Lower Werfen Formation, Kopaonik area (7486570/4795890).
b – Calcite-mylonite attributed to the Steinalm Formation (Anisian), Studenica quarry. c – Polymictic breccia overlying the Steinalm
Formation, Studenica quarry. d – Tuffite, presumably Anisian / Ladinian boundary, Studenica quarry, thin-section crossed polarizers.

Fig. 6. Lithofacies of Kopaonik Formation, Middle to Late Triassic, along road from Brzeće to Kopaonik. a, b – Intensely deformed and
slightly contact-metamorphic grey, hemipelagic limestones with bands of diagenetic replacement chert (now quartzite). c – Graded fine-
grained calcarenite, with diagenetic replacement chert, only weakly deformed. d – Chevron-type folds in a limestone-marl succession with

SCHEFER et al.

Fig. 7. Microfacies of the ?Upper Ladinian to (Lower) Carnian fine-grained hemipelagic grey limestones in the Kopaonik region (Brzeće)
and of the Lower Norian grey micritic and partly cherty limestones of Studenica section. A – Laminated micritic limestone, strongly re-
crystallized. All fossil remnants are destroyed by recrystallization due to metamorphic overprint. The preserved laminae probably indicate a
low engergy turbiditic character of sedimentation and less bioturbation. Sample SRB 113. B – Relatively homogeneous micritic limestone
with less content of clay and pyrite, recrystallized. Sample SRB 115. C – Relatively homogeneous micritic limestone with pyrite. Some
ghosts of organisms resemble filaments and radiolarians and probably peloids. Sample SRB 116. D – Partly some ghost of organisms are
visible, problably representing remnants of crinoids and radiolarians. Sample SRB 115. E – The contact between the light and dark grey
biomicrite is relatively sharp. The dark grey biomicrite is much richer in organisms, partly the shape of radiolarians is relatively well pre-
served. The dark grey biomicrite represents a more condensed facies in comparison with light grey micrite indicating highstand shedding.
Sample SRB 150. F – Ghosts of radiolarians and filament-remnants occur mostly in the very fine-grained turbidites. Sample SRB 153.
G – Overview showing the alternation of relatively organism-free light grey micrite and organism enriched more condensed dark grey
biomicrite. Sample SRB 153. H – Fig. E enlarged. Most organism/components are completely recrystallized and occur only as ghosts.

In section Gradac 2 the Werfen Formation is more calcare-

ous and less sandy. In the lower part there is a rhythmic strati-
fication on a small scale: centimeter-thick layers of limestone
are intercalated with pelitic material that becomes more abun-
dant  up-section,  leading  to  a  purely  pelitic  sequence.  These
pelitic layers are pale green with a silvery shine due to the rel-
atively  higher  degree  of  metamorphism  compared  to  section
Gradac 1. The deformation, characterized by a pervasive bed-
ding-parallel  foliation  and  by  isoclinal  folding,  is  also  more
intense than in section Gradac 2.

In the Kopaonik area, the Werfen Formation is again char-

acterized  by  a  rhythmic  bedding  pattern  of  non-calcareous
shales,  partly  calcite-cemented  sandstones  and  marlstones.
Dynamically grown well-oriented biotite flakes, grown during
regional  metamorphism,  define  a  bedding-parallel  foliation
visible in thin-section. In the immediate vicinity to the intru-
sion  where  contact  metamorphism  is  accentuated,  the  abun-
dance of calcareous beds diminishes (Egli 2008).

Shallow-water carbonates (‘Wurstelkalk’; Gutenstein and
Steinalm Formation equivalents)

The transition from the Werfen Formation into massive

dark metalimestones is particularly well visible in section Gra-
dac 1.  Several  meters  of  bioturbated,  well-bedded  grey  to
brownish  weathering  limestones  are  reminiscent  of  the  basal
Gutenstein  Formation  (‘Wurstelkalk’)  of  the  Eastern  Alps
(Tollmann 1976) or the Szinpetri Limestone Formation in the
Silica nappes (Aggtelek Unit, Hungary) of the Inner Western
Carpathians  (Hips  2006).  Up-section,  these  sediments  give
way to massive, dark grey to nearly black, slightly metamor-
phic limestones with quartz veins (middle to upper Gutenstein
Formation equivalent).

In section Gradac 2 (Fig. 3b), these rocks are strongly de-

formed, and bioturbation is no longer visible in the lower part
of the succession. The marbles show a distinct spaced cleav-
age of centimeter to decimeter size and a N—S-oriented
stretching lineation. Fissures filled with quartz and calcite are
oriented perpendicular to the foliation. Calcite marble, proba-
bly belonging to the Gutenstein Formation, is followed by
massive dolomitic marble of light grey colour with chaotic fis-
sures without foliation. The latter is interpreted as shallow-wa-
ter carbonate of the Steinalm Formation.

Dolostones reminiscent of the Steinalm Formation define

the lowermost part of the Studenica section. The dolostones
are massive, however, and no cleavage is visible. These dolo-

stones are followed by a several tens of meters thick sequence
of  calcite  marble.  These  marbles  are  strongly  deformed  and
mylonitized  (Fig. 5b),  showing  an  alternation  of  differently
coloured domains. An intense stretching lineation is NW—SE
oriented. Minor amounts of dolomite are also found in the cal-
cite marbles, dolomitic layers being less deformed and boudi-
naged,  which  leads  to  the  development  of  sigma-clasts
exhibiting top-to-the-north shear senses (Egli 2008).

In the Kopaonik area the marbles derived from shallow-wa-

ter limestones reach a thickness of a few decameters; often
they are only present as small layers or they may even be com-
pletely missing. The grain size of the marbles increases with
the vicinity to the Kopaonik intrusion. The usually dark-co-
loured sediments pass into white coarse-grained marbles.

Breccia horizon in the uppermost Steinalm Formation
equivalent

Only in the Studenica section, intercalated within the upper-

most Steinalm Formation equivalent, limited to the quarry and
wedging out towards the street (Fig. 3a), a layer of breccias of
about 4 m thickness can be observed. The polymictic breccia
is poorly sorted and consists of clasts one millimeter to several
centimeters  across  (Fig. 5c).  Rounded  to  sub-angular  lime-
stone  clasts  dominate,  dolomite-marble  clasts  are  rare.  The
matrix  consists  of  red  and  greenish  tuffites  with  a  strong
cleavage. Such tuffites may also occur as clasts in this breccia.
The  matrix  becomes  calcitic  towards  the  top  of  the  breccia,
and  is  finally  marly  in  the  uppermost  part.  Isolated  quartz
grains and dynamically grown micas are also found in the ma-
trix. Relics of probable foraminifers and pellets suggest a shal-
low-water origin of some of the components. The competence
contrast  between  the  different  components  causes  heteroge-
neous deformation, which results in an undulating appearance
and stretching lineations visible on the foliation planes. Strain
analysis  (Egli  2008)  after  Ramsay  &  Huber  (1983)  suggests
thinning to 25 % of the original thickness for the breccia hori-
zon.  This  value  is  considered  representative  for  the  entire
Studenica section, except for the dolomitic part at the base.

Tuffites and metabasalts

Intensely foliated tuffites, overlying the Steinalm Forma-

tion equivalent and with an intercalated breccia horizon at
their top, can be observed only in the Studenica section.
Their thickness is about 5 m. These tuffites of red and green

SCHEFER et al.

Sample No. (Coord. MGI)

Conodont fauna

Age

CAI-values

Županj 1

(sample-nr. on Fig. 2)

SRB 110 (7476443/4807045)

Norigondolella sp.
Epigondolella sp. (abneptis-group)

Early–Middle Norian

5.5–6.0

Županj 2 (sample-nrs. on Fig. 2)

SRB 111 (7477694/4806995)

Neogondolella cf. excelsa
Neogondolella cf. eotrammeri
Neogondolella cf. cornuta

Late Anisian

5.5–6.0

SRB 112 (7477694/4806995)

Neogondolella cf. inclinata
(or M. polygnathiformis)

Ladinian–(Carnian) 5.5–6.0

Brzeće (Fig. 4)

SRB 113 (7489302/4796146)

Metapolygnathus cf. polygnathiformis

Carnian (5.0–)5.5

and

6.5–7.0

SRB 114 (7489269/4796084)

Neogondolella sp.

?Ladinian–Carnian

5.5

SRB 115 (7489107/4796221)

Metapolygnathus polygnathiformis

Carnian 5.5–6.0

Studenica (7463291/4814897, Fig. 3)

A 4562

Epigondolella quadrata

Lacian (high 1 to 2)

5.5–6.0

A 4563

Norigondolella sp.
Epigondolella sp.

Norian 5.5–6.0

A 4564

Epigondolella sp. indet
Neohindeodella triassica

Norian 5.5–6.0

SRB 150

Norigondolella navicula
Norigondolella cf. hallstattensis
Epigondolella cf. triangularis

Lacian 2

5.5–6.0

SRB 153

Norigondolella navicula
Norigondolella cf. hallstattensis
Epigondolella sp. indet

Lacian 2

5.5–6.0

Table 1: Triassic conodont faunas of the Kopaonik and Studenica areas, southern Serbia.

colour are similar to those in the matrix of the underlying
breccias (Fig. 5d). These rocks consist mainly of mica with
some up to millimeter-sized clasts of quartz, dolomite, cal-
cite and feldspar. According to Sudar (1986) these volcano-
clastic sediments in the inner Dinarides were deposited near
the Anisian-Ladinian boundary and up to the end of the Ear-
ly Ladinian.

Kopaonik Formation

In the Studenica section and in the Kopaonik area, the shal-

low-water carbonates of the Middle Triassic and the associated
tuffites are overlain by thin-bedded metalimestones with bands
and nodules of chert (Fig. 6a,b). We refer to this formation as
the Kopaonik Formation based on the following definition:

Derivatio nominis: After Kopaonik Mountain area (SW

Serbia). Compare ‘Central Kopaonik Series’ of Sudar (1986)
and Sudar & Kovács (2006).

History: See chapter on geological setting and metamor-

phism.

Definition: Bedded, hemipelagic grey metalimestones, in

certain stratigraphic intervals including fine-grained calcareni-
tes  consisting  of  shallow-water  components;  chert  nodules
and/or  marly  and  clayey  intercalations  are  frequent  (Fig.  7).
The  area  of  deposition  appears  to  be  far  from  shallow-water
ramps or platforms.

Type area: Kopaonik thrust sheet and Studenica slice. A

complete type section cannot be defined because deformation
and metamorphism are too intense in the Kopaonik area. The
formation overlies the shallow-water carbonates of the equiva-
lents of the Steinalm Formation and is overlain by red hemipe-
lagic limestones of probable Jurassic age.

Other localities: Smrekovnica limestones, ‘Metamorphic

Trepča Series’, southern Kopaonik Mountain area, Kosovo
(Sudar 1986; Sudar & Kovács 2006).

Age: Latest Anisian to (Late) Norian, defined by conodonts

(this paper, Sudar 1986 and Sudar & Kovács 2006).

Facies: Grey hemipelagic basinal metalimestones with fine-

grained redeposited calcarenites (deposited by low-density
turbidity currents).

Differences to other and similar formations: The Kopa-

onik Formation is in parts similar to the Gučevo Limestone
Formation  (Sudar  1986;  Filipović  et  al.  2003)  or  to  the
Grivska Formation (Dimitrijević 1997). However, the hemi-
pelagic  metalimestones  of  the  latter  include  significantly
more shallow-water debris from nearby carbonate platforms.
By  contrast,  the  hemipelagic  condensed  or  grey  metalime-
stones of the Kopaonik Formation and the classical Hallstatt
Limestones are devoid of coarser re-deposited shallow-water
turbidites.

Remarks: The succession resembles that of the grey Hall-

statt facies occurring within the Reifling and Pötschen Forma-
tions  of  the  Eastern  Alps  (e.g.  Lein  1987)  as  well  as  the
Felsötárkány  Limestone  Formation  of  the  Bükk  Mountains,
NE Hungary (Kozur 1991; Less et al. 2005). In addition, simi-
lar facies have been described from different locations in the
internal Dinarides without specific formational names (Ramp-
noux 1974; Charvet 1978). A similar succession with hemipe-
lagic Middle/Upper Triassic metalimestones was described in
Korabi/Pelagonia  units  of  eastern  Albania  (Meco  &  Aliaj
2000; Gawlick et al. 2008).

In the Studenica section, the Steinalm Limestones are sepa-

rated from the Kopaonik Formation by sparse outcrops of

STRATIGRAPHY OF TRIASSIC METASEDIMENTS IN THE INTERNAL DINARIDES (SERBIA)

Fig. 8.

Metamorphosed and deformed conodonts with Conodont Colour Alteration (CAI) values 5.5—6.0 from the Studenica section (Sample

SRB150). These conodonts occur in grey cherty metalimestones and are of Early Norian (Lacian) age. 1a – Ductilely deformed Norigondolella
navicula. In this view the original ornamentation on the platform surface looks undeformed. 1b – Platform end of Norigondolella navi-
cula, enlarged, showing complete recrystallization of the original ornamentation by apatite crystal growth. 1c – Enlarged detail of 1b
showing the growth of the apatite crystals. Corrosion is missing. 2a – Slightly deformed Epigondolella triangularis. 2b – Enlarged platform
end showing the complete and relatively homogeneous recrystallization of the conodont. 2c – Enlarged detail showing the growth of apa-
tite crystals. 3a – Ductilely deformed Norigondolella navicula. 3b – Recrystallized fabric, enlarged from 3a. 4a – Deformed and recrystal-
lized part of ?Norigondolella navicula. The original ornamentation on the platform surface is preserved and looks undeformed. 4b – Enlarged
view on the ornamentation showing complete recrystallization of the ornamentation. 5a – Undeformed but totally recrystallized Epigondolella
triangularis. 5b – Recrystallized fabric, enlarged from 5a.

grey-weathering calcite mylonites (‘grey mylonites’) with a
strong cleavage and with a few intercalated pelitic layers
(Fig. 6c). In thin-section, the calcite grains are elongated and
form sigma-clasts indicating top-to-the-northwest shear-sense.
The white marbles overlying the mylonites are reminiscent of
the Steinalm marbles found lower down in the Studenica sec-
tion. However, the mylonites (sample SRB 153, Fig. 3a), the

white  marbles  (sample  A 4564),  and  the  overlying  well-bed-
ded  metalimestones  with  chert  nodules  (samples  A 4563,
SRB 150, A 4562, Table 1) include Norian conodonts (Figs. 8
and 9, Table 1). The conodont faunas cover only a very short
time interval of the Early Norian, ranging from the higher part
of the Lacian 1 or basal Lacian 2 (Epigondolella quadrata) to
the  Lacian 2  (Epigondolella  triangularis  and  Norigondolella

101

STRATIGRAPHY OF TRIASSIC METASEDIMENTS IN THE INTERNAL DINARIDES (SERBIA)

hallstattensis).  Because  some  important  details  of  the  con-
odont morphology were destroyed by intense deformation and
low-grade  metamorphism  (CAI-values  between  CAI 5.5  and
6.0),  the  determination  of  the  conodonts  species  cannot  be
more precise.

The conodont data from the grey calcite-mylonites, that is

from the Early Norian age pose a problem: obviously Ladin-
ian and Carnian strata are missing in the Studenica section. As
a primary stratigraphic gap by non-deposition and/or erosion
appears unlikely to be the case, we suggest a tectonic contact
along the calcite-mylonites.

In the Gradac 2 section, the Kopaonik Formation consists of

thin-bedded marbles with interbedded marls. Weathering and
fresh surfaces of the marbles are dark; the intercalated pelitic

Fig. 10. Metamorphosed and ductilely deformed conodonts (Metapolygnathus polygnathiformis) with Conodont Colour Alteration (CAI) val-
ues in average CAI 5.5—6.0 from Kopaonik, Brzeće section (sample SRB 115). These conodonts come from probably Upper Carnian grey
metalimestones. 1a – Strongly recrystallized and corroded specimen. CAI 5.5—6.0. 1b – Platform end enlarged showing strong recrystalliza-
tion and growth of the apatite crystals. 1c – Enlarged detail with strong recrystallization and partial corrosion of the surface. 1d – Detail of
the surface with relatively large apatite crystals. 2a – Strongly recrystallized and slightly deformed specimen. CAI 6.0. 2b – Platform end
enlarged showing strong recrystallization and growth of the apatite crystals. The original surface is completely destroyed by recrystalliza-
tion. 2c – Enlarged detail showing strong recrystallization and growth of individual apatite crystals. 2d – Enlarged detail showing strong
recrystallization of apatite and enlargement of the crystallites.

layers are yellowish. After a few meters of rhythmic alterna-
tions the metalimestones and marls give way to metalime-
stones with chert layers.

In the type area (Fig. 4), the Kopaonik Formation makes up

large cliffs and the most conspicuous outcrops. The formation
is  well  stratified;  calcareous  beds  alternate  with  chert-rich
metalimestones  or  marly  intercalations.  The  thickness  of  the
beds  varies  between  centimeters  and  decimeters  (Fig. 6d).
Where  marly  layers  are  absent,  the  chert  layers  and  nodules
are diagnostic for this formation. Weathered surfaces are grey-
ish to brownish, depending on the amount of clay. In the vi-
cinity of the intrusion, the Kopaonik Formation is transformed
into  massive  skarns  and  hornfelses  due  to  contact  metamor-
phism (Fig. 6e). Metamorphosed chert layers and calcsilicates

103

STRATIGRAPHY OF TRIASSIC METASEDIMENTS IN THE INTERNAL DINARIDES (SERBIA)

mis is destroyed by extreme polyphase deformation and (low-
grade) metamorphism (CAI-values of CAI 5.5—6.0, reaching
locally CAI 6.5—7.0, Fig. 10).

Two successions of metalimestones within the Kopaonik

Formation are developed in the wider area of Kovači village,
that  is  in  Županj  hamlet  (north  of  the  road  from  Jošanička
Banja  towards  Biljanovac).  In  the  locality  Županj 1  an  Early
to  Middle  Norian  conodont  fauna,  including  Norigondolella
sp. and Epigondolella sp. could be isolated from dark grey mi-
critic  limestone  beds  (sample  SRB 110  in  Fig. 2,  Table 1).
These  micritic  metalimestones  overlie  a  thick  series  of  dark
grey, bedded metalimestones with fine-grained siliciclastic in-
tercalations.  In  the  locality  Županj 2  (samples  SRB 111,  112
in Fig. 2) a stratigraphically reduced series of dark grey cherty
and deformed metalimestones is dated as Late Anisian by the
occurrence  of  Neogondolella  cf.  excelsa  and  Neogondolella
cf.  cornuta, and, higher up, as Late Ladinian/?Early Carnian
by  the  occurrence  of  Neogondolella  cf.  inclinata.  Due  to  the
strong  deformation  of  the  conodonts  a  determination  as
Metapolygnathus  polygnathiformis  also  seems  possible
(Fig. 11, Table 1). This locality is of special interest because it
provides evidence of Middle Triassic (Late Anisian to Ladin-
ian?)  hemipelagic  grey  metalimestones  in  the  Kopaonik  re-
gion  for  the  first  time.  Near  to  our  samples  from  Županj 2,
Sudar (1986) found several Carnian conodonts.

Red hemipelagic limestones and radiolarites

Only in the Studenica section are such younger sediments

exposed. Here, the Kopaonik Formation is overlain by red to
violet  hemipelagic  limestones  with  a  thickness  of  only  1—2
meters  showing  a  strong  penetrative  foliation.  Limestone
laminae, only up to one millimeter in thickness, are separated
by  thin  films  of  clay  and  occasional  white  marble  layers.  In
thin-section accessory quartz grains and relics of radiolarians
are visible. These red hemipelagic limestones probably repre-
sent  an  equivalent  of  the  Middle  Jurassic  condensed  Klaus
Limestone  of  the  Eastern  Alps  and  Western  Carpathians
(Krystyn 1971; Tollmann 1976; Gawlick et al. 2009a), or of
the Toarcian—Middle Jurassic Rosso Ammonitico of the inter-
nal  Hellenides  (e.g.  Baumgartner  1985).  Similar  condensed
red  Bositra  limestones  of  Middle  Jurassic  age  below  sili-
ceous sedimentary rocks were recently described also in SW
Serbia  (Radoičić  et  al.  2009).  They  are  followed  up-section
by  some  meters  of  metamorphosed  massive  radiolarites  of
supposed late Middle to Late Jurassic age.

Ophiolitic mélange

An ophiolite-bearing mélange of considerable thickness tec-

tonically  overlies  the  Triassic—Jurassic  succession  in  the
Studenica section. In the Kopaonik area, the mélange is thrust
on top of the Kopaonik Formation while the sections Gradac 1
and  Gradac 2  do  not  expose  the  contact  to  the  mélange.  The
mélange contains, embedded in a brown to reddish mud ma-
trix,  blocks  predominantly  of  serpentinite;  basalts,  turbiditic
sandstones  and  carbonate  rocks  are  also  found  as  blocks.  In
the  Studenica  section  the  mélange  is  often  foliated  due  to  a
strong younger tectono-metamorphic overprint.

Regional correlation and reconstruction of the

original sedimentary succession

Based on lithofacies and age dating we can correlate both

the  intensely  folded  strata  of  the  Kopaonik  area  with  the  not
visibly folded yet strongly foliated and metamorphosed strata
from  the  sections  Studenica  and  Gradac 1  and  2  (Fig. 12).  It
appears  that  all  our  sections  are  stratigraphically  incomplete
due  to  intense  deformation  leading  to  the  thinning  of  strata.
Hence each of the sections only reveals a part of what might
be considered an originally complete stratigraphic succession
for the study area.

According to our stratigraphic interpretation of the

Studenica section, Ladinian as well as Carnian sediments are
clearly missing in this section because the Anisian—Ladinian
boundary  tuffites  are  directly  overlain  by  marbles  yielding
Norian  (Lacian 1—2)  conodonts  that  we  attribute  to  the
Kopaonik  Formation.  This  omission  of  strata  could  have
been caused by normal faulting; however, we were unable to
detect normal faults in this section. On the other hand, strong
penetrative deformation has reduced marbles and limestones
in the Studenica section to 25 % of their original thickness as
shown by a representative strain analysis of the breccia hori-
zon (Egli 2008).

During mapping of the Kopaonik area, all Anisian shallow-

water carbonates identified in the other profiles were included
into  one  single  formation  (‘shallow-water  carbonates’  in
Fig. 4)  because  the  succession  is  in  most  places  too  thin  (or
even  lacking)  to  allow  a  subdivision  into  Gutenstein  and/or
Steinalm  Formation.  In  this  area,  these  formations  are  either
stratigraphically reduced or tectonically thinned, or both.

In the Kopaonik area and in the section Gradac 2 the Kopa-

onik Formation mostly consists of typical fine-grained calcilu-
tites with interbedded marls, cherty layers and nodules and
calcarenites with some shallow-water material derived from a
carbonate platform.

The overall sedimentary evolution of the Kopaonik Forma-

tion in the type-area can be summarized as follows: after shal-
low-water carbonate sedimentation prevailing during most of
the Anisian, hemipelagic sedimentation started with a relatively
thin succession of Upper Anisian to Ladinian grey cherty
limestones that pass into a thick series of Lower Carnian lime-
stones with some marls and few cherts, followed by Upper
Carnian to Lower Norian micritic limestones with an increase
of cherts in the Middle Norian.

In the Studenica section the Kopaonik Formation is overlain

by Jurassic hemipelagic limestones and radiolarites. These Ju-
rassic sedimentary rocks occur a few meters above the Norian
(Lacian 1—2) conodont-bearing horizon and testify to continu-
ing subsidence of the distal continental margin before obduc-
tion  of  the  ophiolites.  In  addition  to  continuing  subsidence,
shallowing  of  the  calcite  compensation  depth  (CCD)  in  the
Middle—Late  Jurassic,  brought  about  by  changes  in  plankton
productivity, export of carbonate mud from adjacent platforms
and  in  other  paleoceanographic  variables  (e.g.  Bernoulli  &
Jenkyns  2009),  might  have  led  to  deposition  of  radiolarites
near or below the CCD. The age of the distal continental-mar-
gin radiolarites is generally dated as Middle Jurassic in the in-
ternal  Dinaride—Hellenide  realm  (e.g.  Baumgartner  1985;

105

STRATIGRAPHY OF TRIASSIC METASEDIMENTS IN THE INTERNAL DINARIDES (SERBIA)

mélanges below the ophiolites. In the closer Kopaonik region,
however,  sediments  younger  than  the  Kopaonik  Formation
were  not  found  below  the  ophiolitic  mélange,  probably  be-
cause  obduction-related  thrusts  cut  across  older  formations
in this area.

Combining the four stratigraphic sections correlated in

Fig. 12 with the other outcrops and the conodont data allows
us  to  draw  a  reconstructed  synthetic  stratigraphic  succession
from the Upper Paleozoic up to the Upper Cretaceous show-
ing the overall facies evolution (Fig. 13). Overlying an Upper
Paleozoic  basement,  the  some  100 m  thick  sedimentary  suc-
cession  starts  with  siliciclastic  sediments,  comparable  to  the
Werfen  Formation.  A  Late  Permian  onset  of  sedimentation
cannot  be  excluded.  Carbonate  production  started  with  the
uppermost Werfen Formation, perhaps during the late Early
Triassic, as in the Southern or Eastern Alps. The Middle Trias-
sic sequence starts with shallow-water carbonates (Gutenstein
and  Steinalm  Formation  equivalents),  followed  by  Upper
Anisian  hemipelagic  sediments  in  the  wake  of  the  drown-
ing of the Steinalm ramp/platform. Hemipelagic carbonate
sedimentation  is  proven  for  nearly  the  entire  Middle  and
Late  Triassic.  The only preserved Jurassic sediments in the
area consist of pelagic red metalimestones and radiolarites of
probably Middle—?Late Jurassic age. These are followed by
a  ?Middle—Upper  Jurassic  ophiolitic  mélange  and  the  over-
riding West Vardar Ophiolites. From this reconstructed strati-
graphic  succession,  where  original  thicknesses  are  estimated
based on a representative strain determination (Egli 2008),
it becomes clear that the original thickness of the Kopaonik
Formation is at least 400 meters. In the Kopaonik area, this is
also  apparent  from  the  large  outcrop  areas  appearing  on  the
geological map (Fig. 4).

Discussion

Before discussing the paleogeographic setting of our study

area in a wider context within the Alps-Carpathians-Dinarides
system  we  compare  the  stratigraphy  and  facies  of  the  study
area  with  that  of  other  parts  of  the  Dinarides.  The  Mesozoic
stratigraphy  is  rather  well  established  in  the  more  external
units,  namely  in  the  main  parts  of  the  Drina-Ivanjica  thrust
sheet  southwest  of  our  study  area  (=  ‘Zone  de  Golija’  of
Aubouin  et  al.  1970)  and  in  the  East  Bosnian-Durmitor
thrust sheet (= ‘Zone Serbe’ of Aubouin et al. 1970), based
on  the  work  of  Cadet  (1970,  1978),  Charvet  (1970,  1978),
Rampnoux  (1970,  1974),  Sudar  (1986),  Dimitrijević  &
Dimitrijević  (1991),  Dimitrijević  (1997)  and  Sudar  et  al.
(2008). In these areas a first platform-drowning event, which
follows shallow-water carbonate sedimentation of the Guten-
stein  and  Steinalm  Formations  is  also  recorded  during  the
latest  Anisian  by  the  onset  of  condensed  red  pelagic  lime-
stones  (Bulog  Limestone  of  Rosso  Ammonitico-type),  first
described by Hauer (1888, 1892). This facies is usually fol-
lowed by volcanic tuffs that often occur around the Anisian/
Ladinian boundary (Sudar 1986).

In our study area, the transition from shallow-water to hemi-

pelagic sedimentation coincides with the occurrence of a brec-
cia below the main tuffite horizon in the Studenica section. A

Fig. 13.  Synthetic  sedi-
mentary  succession  com-
bining  the  stratigraphic
columns  of  Fig. 12  a—d.
The  thicknesses  are  cor-
rected for tectonic thinning
according to the method of
Ramsay & Huber (1983).

similar breccia horizon (‘Podbukovi Conglomerate Member’)
is observed in the uppermost Anisian dolomitic limestones of
the  Jablanica  Formation  (an  equivalent  of  Steinalm  Lime-
stone)  of  the  Jadar-Kopaonik  thrust  sheet  (i.e.  in  the  ‘Jadar
Block Terrane’ of Filipović et al. 2003). In the same area this
breccia  horizon  is  overlain  by  volcanics  (metaandesites  and
accompanying pyroclastics of the Tronoša Formation).

According to our conodont data from Županj localities, the

drowning in the Kopaonik area occurred during the latest Ani-
sian  (Fig. 13).  Occasional  calcarenites  with  shallow-water
components  in  the  ?Lower  Carnian  succession  suggest  rede-
position  of  carbonate  material  derived  from  carbonate  plat-
forms, together with shedding of fine carbonate silt and lutum

106

SCHEFER et al.

from the platforms during sea-level highstands (Schlager et al.
1994).  This  may  explain  the  relatively  high  sedimentation
rates  during  this  time  interval.  A  hemipelagic/deep-benthic
setting,  equivalent  to  the  grey  Hallstatt  facies  of  the  Eastern
Alps—Western  Carpathians  (Lein  1987)  is  in  line  with  the
faunal content (radiolarians, conodonts, pelagic bivalves).

The most important facies difference with respect to the

more external parts of the Drina-Ivanjica thrust sheet (includ-
ing  strata  within  so-called  ‘olistoplaka’,  which  Dimitrijević
(1997)  interpreted  as  gravitationally  emplaced  olistoliths  and
that we regard as an integral part of the Drina-Ivanjica thrust
sheet)  and  part  of  the  East  Bosnian-Durmitor  thrust  sheet  is,
that the strata found up-section from the Bulog Limestone and
the  tuffites  are  typically  shallow-water  carbonate  sequences,
and so equivalents of the Upper Ladinian to Carnian Wetter-
stein and the Norian to Rhaetian Dachstein formations (Dimi-
trijević  &  Dimitrijević  1991;  Sudar  et  al.  2008).  In  some
localities within these two more external thrust sheets, howev-
er,  a  base-of-slope  to  basinal  hemipelagic  facies  of  poorly
known  age  (Middle  to  Late  Triassic  and/or  Early  to  Middle
Jurassic?)  develops,  that  resembles  the  Kopaonik  Formation
(Fig. 13).  It  also  consists  of  detrital  carbonate  and  siliceous
sediments and was referred to as Grivska Formation by Dimi-
trijević (1997). In the more external East Bosnian—Durmitor
thrust sheet Rampnoux (1970, 1974) described a similar ba-
sinal facies, his ‘calcaires lités pélagiques

silex’, for exam-

ple  from  the  ‘sillon  de  Zlatar’,  which  should  be  bordered,
according to this author, by Wetterstein- and Dachstein-type
platforms.  The  Grivska  Formation  and  the  age-equivalent
Wetterstein and Dachstein platforms are overlain by Jurassic
hemipelagic limestone and radiolarites (Djerić et al. 2007a,b;
Vishnevskaya et al. 2009) similar to those above the Kopaon-
ik Formation in the Studenica section, followed by the ophi-
olitic  mélange.  Carnian  to  Norian  cherty  limestones  with
conodonts (Gučevo Limestone) were also described from oth-
er  parts  of  the  Jadar-Kopaonik  thrust  sheet  (‘Jadar  Zone’  of
Sudar 1986, ‘Jadar Block Terrane’ of Filipović et al. 2003).

In spite of some lithological similarities between the Grivska

and  the  Kopaonik  Formation  we  like  to  emphasize  that  the
limestone  succession  of  the  Grivska  Formation  includes  sig-
nificantly more shallow-water debris from the nearby Ladin-
ian to Rhaetian carbonate platforms. In addition, the Grivska
Formation appears to be restricted to the more external paleo-
geographic domain (the Drina-Ivanjica and the East Bosnian-
Durmitor thrust sheets). Moreover, Bulog-type limestones and
equivalents of the Wetterstein and Dachstein Formations were
not  found  in  our  area.  All  this  suggests  that  the  grey  hemi-
pelagic sequences of the Kopaonik Formation, though yielding
fine-grained shallow-water debris, represent a more distal fa-
cies of the Adriatic margin.

A paleogeographic position of the facies of the Kopaonik

Formation  at  the  distal  Adriatic  margin  adjacent  to  the  Neo-
tethys  (i.e.  the  Meliata-Maliac-Vardar  Ocean)  becomes  even
more convincing when we compare our area with the Eastern
Alps and the Albanides—Hellenides. In the Northern Calcare-
ous  Alps  of  Austria  (Lein  1987)  and  the  Korabi-Pelagonia
zone  in  Albania  (Meco  &  Aliaj  2000;  Gawlick  et  al.  2008),
similar  deposits  are  interpreted  to  have  been  deposited  in  a
distal continental margin position (Haas et al. 1995; Gawlick

et al. 1999, 2008) after rifting began during the Late Pelsonian
leading  to  the  opening  of  the  Neotethys  (Vardar-Meliata
branch  of  Velledits  2006).  The  Kopaonik  Formation  also  re-
sembles  the  so-called  ‘grey  Hallstatt  facies’  or  Zlambach  fa-
cies zone (Pötschen Limestone) of the Eastern Alps (e.g. Lein
1987;  Gawlick  2000).  It  further  resembles  the  Felsötárkány
Limestone  Formation  in  the  Bükk  Mountains  (Kozur  1991;
Less et al. 2005), as well as coeval deep-water limestones in
the Korabi-Pelagonian zone of Albania (Gawlick et al. 2008).
A  paleogeographic  derivation  of  the  Kopaonik  Formation
close to the Meliata-Maliac-Vardar branch of the Neotethys is
also  suggested  by  the  similarity  with  the  Adhami  Limestone
that occurs in the distal part of the internal Pelagonian conti-
nental margin in the Argolis area of Greece and separates the
shallow-water platforms (Pantokrator Limestone) of the more
proximal margin from the oceanic realm (Baumgartner 1985).

Almost all the occurrences of Middle to Upper Triassic

chert-rich deep-water limestones occur on the distal parts of
the  continental  margin  facing  the  Meliata-Maliac-Vardar
Ocean. Towards the more proximal areas of the margin, the
sites  of  hemipelagic  deposition  were  linked  to  coeval  car-
bonate  platforms  (Wetterstein,  Dachstein  platforms).  The
depositional area of the Kopaonik Formation must also have
been  connected  to  one  or  more  Middle  to  Upper  Triassic
rimmed  carbonate  platforms,  like  those  preserved  in  the
more external parts of the Dinarides, whereby the grain size
and amount of the redeposited material decreases distally as
can  be  observed  from  the  Durmitor  area  across  the  Drina-
Ivanjica  zone  to  the  Kopaonik  area.  Other  carbonate  plat-
forms  may  have  been  present  along  the  ocean—continent
boundary,  the  deeper  areas  forming  embayments  like  the
modern Tongue of the Ocean. However, there seems to exist
a  general  trend  from  the  external  to  the  internal  Dinarides
from  shallow-water  to  pelagic  near-oceanic  environments.
Applying Occam’s Razor (Thorburn 1918), we opt for a sim-
ple  continental  margin  model.  In  fact,  the  paleogeographic
location  of  the  Jadar-Kopaonik  thrust  sheet  is  analogous  to
that of the Hallstatt facies of the Eastern Alps and to that of
the depositional areas of similar facies in Albania or Greece
adjacent  to  oceanic  units  attributed  to  the  Meliata-Maliac-
Vardar branch of the Neotethys and may represent the most
distal parts of the Adriatic continental margin. Our data are
consisted with the one-ocean-hypothesis and an origin of all
ophiolites, including the so-called Dinaridic ophiolites, from
east of the Drina-Ivanjica and Kopaonik units.

Conclusions

The metamorphic sedimentary succession of the Jadar-

Kopaonik  thrust  sheet  in  the  most  internal  Dinarides  of
southern Serbia includes a succession from the Upper Paleo-
zoic  terrigenous  sediments  to  the  Upper  Jurassic  ophiolitic
mélange and the Western Vardar ophiolites obducted in the
Late  Jurassic.  Lower  Triassic  siliciclastics  and  limestones
are overlain by Anisian shallow-water carbonates. A drown-
ing event during the latest Anisian resulted in the deposition
of a grey hemipelagic limestone succession characterized by
fine-grained  redeposited  and  often  silicified  calcarenites,

107

STRATIGRAPHY OF TRIASSIC METASEDIMENTS IN THE INTERNAL DINARIDES (SERBIA)

shed  by  low-density  turbidites  from  a  carbonate  platform.
New conodont faunas date this hemipelagic sequence as Late
Anisian  to  Norian,  possibly  extending  into  the  Early  Juras-
sic, which makes it to an equivalent of the grey Hallstatt fa-
cies  of  the  Eastern  Alps.  The  younger  sediments  overlying
the Kopaonik Formation are red hemipelagic limestones and
radiolarites of probably Middle—Late Jurassic age; they sug-
gest that deep-pelagic conditions preceded the obduction of
the Western Vardar Ophiolitic Unit.

Sedimentation of the hemipelagic Kopaonik Formation

was  contemporaneous  with  shallow-water  carbonate  produc-
tion in nearby carbonate platforms that were part of the same
passive continental margin. Most of these platforms were lo-
cated  on  the  more  proximal  parts  of  the  Adriatic  margin,
whereas the distal margin was dominated by pelagic and distal
turbiditic  sedimentation,  facing  the  evolving  ocean  to  the
east. Our data are in line with a continental margin model in
which the facies belts are arranged in a logical order from the
proximal  margin  to  the  Neotethys  Ocean.  In  our  interpreta-
tion the Drina-Ivanjica and Kopaonik thrust sheets expose the
most distal portions of the Adriatic margin, emerging in tec-
tonic  windows  below  one  and  the  same  ophiolite  nappe  re-
ferred to as the Western Vardar Ophiolitic Unit (including the
so-called Dinaridic ophiolites) derived from the east and over-
thrusting the Durmitor zone.

We see no evidence for one or several independent Triassic

oceans between the Adria, the Drina—Ivanjica and/or the
Kopaonik areas. The sedimentological and stratigraphic evo-
lution of the different areas reflects the transition from a proxi-
mal to a distal continental margin.

Acknowledgments:  We  thank  S.  Kovács  and  S.  Kövér
(Budapest)  who  participated  in  the  field  campaign  for  their
valuable  discussions  and  support,  and  J.  Charvet  and  J.
Michalík for thoughtful reviews. This project was financed by
the Swiss National Funds, Project No. 200020-109278 to S.M.
Schmid,  B.  Fügenschuh  and  S.  Schefer.  The  research  of  M.
Sudar and D. Jovanović was supported by the Ministry of Sci-
ence and Technological Development of the Republic of Ser-
bia, Project No. 146009.

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