GeolCarp_Vol60_No1_35

GEOLOGICA CARPATHICA, FEBRUARY 2009, 60, 1, 35—41 doi: 10.2478/v10096-009-0004-5

www.geologicacarpathica.sk

Introduction

The investigated area is situated in  western Serbia, in an ex-
tremely  complex  geotectonic  setting  (Fig. 1).  In  the  territory
of  western  Serbia,  there  are  two  belts  of  ophiolitic  mélange
overlain by large ultramafic massifs. The more external belt is
known as the Dinaridic Ophiolites or Dinaridic Ophiolite Belt
(Pamić et al. 2002; Karamata 2006) or as the Central Dinaridic
Ophiolite belt (Lugović et al. 1991). The more internal belt is
referred  to  as  the  Vardar  Zone  Western  Belt  by  Karamata
(2006), but also referred to under a variety of names such as
Inner Dinaridic ophiolite belt (Lugović et al. 1991), External
Vardar  Subzone  (Dimitrijević  1997,  2001)  or  simply  Vardar
Zone (Pamić et al. 2002). These ophiolite belts are separated
by  the  Drina-Ivanjica  Element.  The  majority  of  authors  re-
garded  the  Drina-Ivanjica  Unit  as  a  continental  terrane  that
was  originally  located  between  two  separate  oceanic  basins
(Dimitrijević  &  Dimitrijević  1973;  Robertson  &  Karamata
1994;  Dimitrijević  2001;  Karamata  2006).  Others  postulated
that  this  element  was  formed  by  out-of-sequence  thrusting
from  the  European  margin  (Pamić  et  al.  1998;  Hrvatović  &
Pamić 2005). According to Schmid et al. (2008), Drina-Ivanjica
is a thrust sheet which was probably emplaced in Early to mid-
Cretaceous  times  on  top  of  the  East  Bosnian—Durmitor  thrust
sheet. Like the East Bosnian-Durmitor composite thrust sheet,
the Drina-Ivanjica thrust sheet also carried passively the previ-
ously obducted Western Vardar ophiolites (Zlatibor ophiolites).

Early Senonian radiolarian microfauna and biostratigraphy

from the Western Vardar Zone (Western Serbia)

NEVENKA DJERIĆ

, NATAŠA GERZINA

, VIOLETA GAJIĆ

and NEBOJŠA VASIĆ

Department of Paleontology, Faculty of Mining and Geology, University of Belgrade, Kamenička 6, 11000 Belgrade, Serbia;

djeranen@eunet.yu

Department of Geology, Faculty of Mining and Geology, University of Belgrade, Kamenička 6, 11000 Belgrade, Serbia;

nacy@nadlanu.com

Department of Petrology and Geochemistry, Faculty of Mining and Geology, University of Belgrade, Djušina 7, 11000 Belgrade, Serbia;

sedimentologija@yahoo.com

(Manuscript received February 21, 2008; accepted in revised form June 12, 2008)

Abstract: The studied deposits represent the sedimentary cover of ophiolitic mélange of the Western Vardar Zone Belt.
An association of sediments that correspond to a primary pyroclastic material occurs in the Upper Cretaceous carbonate
sediments near the village of Struganik (Western Serbia). This is an interlayer within mainly carbonate sediments
represented by limestone, clayey limestone and marlstone. It is made of the following succession: a lamina made of
crystalline quartz, sanidine, plagioclase and biotite and a layer of clay. The clay is of the smectite type, highly crystal-
line. The age of the radiolarian assemblage from the clay layer is assigned to Early Senonian, based on the co-occur-
rence of radiolarian taxa: Dictyomitra formosa Squinabol, Dictyomitra koslovae Foreman, Dictyomitra torquata Foreman,
Alievium sp. cf. A. superbum (Squinabol) and Pseudoaulophacus sp. cf. P. venadoensis Pessagno. The pyroclastic
material was brought into the water environment by a cloud that was formed after an explosive eruption whose exact
location cannot be determined at the moment. According to geological data, there are no indications of volcanic activity
before the Late Cretaceous in the wider studied area. Marine sedimentation continued after gravitational differentiation
of pyroclastic material. The results of petrological and sedimentological investigations reveal that Struganik Limestone
originated in a deep-water environment and that the sedimentation area was on the continental slope.

Key words: Upper Cretaceous, NW Serbia, Vardar Zone Western Belt, Radiolaria, pyroclastic, smectite.

Fig. 1. Sketch of the terranes of central and western Serbia (accord-
ing to Karamata et al. 2000) with the position of the studied locali-
ty.  DHCT  –  Dalmatian-Herzegovinian  Composite  Terrane;
CBMT  –  Mid-Bosnian  Mountains  Terrane;  EBDT  –  East-Bos-
nian-Durmitor Terrane; SUT – Sana-Una Terrane; DOB – Dinar-
idic  Ophiolite  Belt  (Terrane);  DIE  –  Drina-Ivanjica  Element
(Terrane);  VZWB  –  Vardar  Zone  Western  Belt;  JBT  –  Jadar
Block Terrane; KBR – Kopaonik Block and Ridge; MVZ – Main
Vardar  Zone;  SMCT  –  Serbo-Macedonian  Composite  Terrane;
black  –  ophiolite  massifs:  b  –  Borje;  i  –  Ibar;  Kk  –  Krivaja-
Konjuh; m – Maljen; o – Ozren; z – Zlatibor.

DJERIĆ, GERZINA, GAJIĆ and VASIĆ

The Jadar Block is considered (by the majority of Serbian

geologists) to be either an integral part of the Vardar Zone
(Dimitrijević 1997) or an exotic body pushed into the Vardar
Zone in the Late Cretaceous (Karamata et al. 1994). Accord-
ing to some recent interpretations, the Drina-Ivanjica and Ja-
dar units structurally underlie Neotethyan ophiolites of
Jurassic age that were obducted onto the Adria margin dur-
ing the Late Jurassic (Schmid et al. 2008).

The present-day tectonic contact between the Drina-Ivanjica

and the Jadar Block is very steep and has a strong dextral strike-
slip component (Gerzina & Csontos 2003). In the literature, this
contact is referred to as the “Zvornik suture” (Dimitrijević
1997) that is supposed to mark the ophiolitic suture between the
continental Drina-Ivanjica and Jadar Block Terranes (Karamata
2006). According to Schmid et al. (2008), the Zvornik “suture”
simply represents the northwestern continuation of the long belt
of Senonian flysch, which marks the tectonic boundary between
the Drina-Ivanjica and Jadar-Kopaonik thrust sheets.

There are opinions that the ophiolites in these two ophio-

lite belts resulted from the obduction of just one ocean (Pa-
mić 1998; Pamić et al. 2000; Csontos et al. 2003; Schmid et
al. 2008). The occurrence of ophiolites in two and not only
in one belt is due to out-of-sequence thrusting and later
nappe refolding during Cretaceous and Cenozoic orogenic
phases (Csontos et al. 2003). The majority of Serbian geolo-
gists, however, are of the opinion that these ophiolitic belts
represent remnants of two different oceanic environments.

In the wider studied area, Cretaceous sedimentation begins

with the Albian transgression. Terrigenous-carbonate and
carbonate sedimentation continued from the Albian to the
Maastrichtian, while flysch sediments were deposited during
the latest Senonian (Filipović et al. 1978).

The aim of this study was to present information on the

Upper Cretaceous radiolarian assemblage from the rocks
which cover the ophiolites of the Vardar Zone Western Belt.

The clay in which radiolarians were found is of volcanic ori-

gin and this is the first finding of smectite clay in Upper Creta-
ceous sediments of Serbia. Due to the tectonic position of the
investigated area, we consider that this paper is an important
contribution to better understanding of the geological evolu-
tion of the area during the Cretaceous, which will enable com-
parison with similar rocks in the surrounding regions.

Geological setting

The wider investigated area is situated in the Vardar Zone

Western Belt (Western Serbia), north of the large ophiolitic
complex of Maljen and Suvobor (Fig. 2). The underlying
ophiolitic mélange was formed due to the closure of the oce-
anic area during the Late Jurassic to Early Cretaceous (Cson-
tos et al. 2003, 2004; Schmid et al. 2008).

The sedimentary cover of the ophiolites in the wider area

of the village of Struganik is represented by the Albian-Cenom-

Fig. 2. Simplified and modified geological map of the wider surroundings of the investigated area with the position of the studied locality
(Struganik quarry), based on the Geological Map of Former Yugoslavia 1 : 500,000. VZWB – Vardar Zone Western Belt, JB – Jadar
Block, DIE – Drina-Ivanjica Element.

EARLY SENONIAN RADIOLARIAN MICROFAUNA AND BIOSTRATIGRAPHY (WESTERN SERBIA)

anian  conglomerates,  conglomeratic  limestone  and  sand-
stone (Filipović et al. 1978; Rabrenović et al. 2002). Cenom-
anian sediments in the area of Struganik are represented by
conglomerate,  conglomeratic-sandy  limestone  and  sand-
stone.  These  sediments  are  concordantly  overlain  by  grey
and bluish marlstone with abundant floral detritus, limestone
and marly sandstone. The uppermost part of the Cenomanian
is mostly made of marlstone with rare intercalations of lime-
stone. The Cenomanian age of the sediments was document-
ed paleontologically and it was based on macrofauna (Ostrea
carinata, Caprinella  triangularis,  Puzosia  planulata,  Acan-
thoceras mantelli, Turilites costatus, etc.; Marković & An el-
ković  1953)  and  microfauna  (Rotalipora  appenninica,  R.
cushmani,  Praeglobotruncana  stephani,  Globigerina  infra-
cretacea; Filipović et al. 1978). Turonian sediments are rep-
resented  by  detritic  limestone  with  intercalations  of
marlstone,  reddish  layered  cherty  limestone,  marly-sandy
conglomeratic  limestone  and  reddish  marly  claystone  with
limestone intercalations. Their Turonian age was document-
ed by microfauna (Praeglobotruncana helvetica, Rotalipora
sp.,  Globotruncana  laparenti  coronata  etc.;  Filipović  et  al.
1978). Senonian sediments are best exposed in the village of
Struganik.  They  are  represented  by  the  so-called  Struganik
Limestone,  a  series  mostly  made  of  thin-layered  limestone,
clayey  limestone  and  marlstone.  Chert  concretions  are
present  in  all  levels.  The  Senonian  age  was  documented  on
the  basis  of  macrofauna  (Inoceramus  balticus,  Inoceramus
lamarcki;  Marković  &  An elković  1953)  and  microfauna
(Globotruncana  stuarti,  G.  tricarinata;  Filipović  et  al.
1978). A layer of green-grey pelitic sediments, which corre-
spond  to  a  primary  pyroclastic  material,  occurs  within  the
Senonian limestone and marlstone (Vasić et al. 2005).

The pyroclastic material was brought into the aquatic envi-

ronment most probably by a cloud that was formed after a
volcanic eruption. Crystalloclasts, as the largest clasts, were
the first deposited from the cloud by gravitational differenti-
ation, forming a lamina. Finer grains, fragments of volcanic
glass in the first place, formed the overlying layer. The vol-
canic glass was transformed into smectite clay by diagenetic
processes (Vasić et al. 2001, 2005).

Petrological characteristics of the Struganik

quarry section

The local lithological column, in which a layer of primary

pyroclastic sediments was noticed, was measured on the lower
level of a quarry in Struganik (coordinates: x – 7428643,
y – 4894326, z – 366 m). The thickness of the column is
11.5 m (Fig. 3).

The autochthonous sediments are platy and bedded car-

bonate rocks with contents of CaCO

(calcite) from 50 to

88 %, which classifies them as marlstone-marly limestone in
the  Bart  classification.  According  to  the  Folk  classification
(Folk 1959), the sediments correspond to micrite, fossilifer-
ous micrite and biomicrite with an association in which glo-
botruncanas,  poorly  preserved  radiolarians  and  silicisponge
spicules  (calcified)  are  conspicuous.  Laminas  (up  to  5 mm
thick)  that  represent  biomicrite  with  dominant  globotrun-

canas were found in marly limestone and marlstone in the
lower part of the column made of micrite. Traces of life ac-
tivity, namely biogenic structural forms, are present on bed-
ding surfaces in these rocks.

The column is composed of four beds (30—75 cm) of lime-

stone,  which  is  defined  as  biosparite,  biointrasparite,  cal-
carenite  and  calcirudite  (Fig. 2).  These  limestones  are
characterized by gradation, horizontal and wavy lamination.
A  thick  limestone  bad  is  characterized  by  continuity  of  the
structures  from  the  lower  to  the  upper  bedding  surface,
which corresponds to the Tb-c succession of the Bouma se-
quence (Bouma 1962) (Fig. 4).

In a lithological sense, graded limestone begins with

coarse-grained  varieties  (calcirudite-calcarenite),  and  ends
with  fine-grained  allochemical-sparry  varieties  (biosparite
and biointrasparite). Paleodictyon structure (Seilacher 2007)
was  noticed  on  the  lower  surface  of  a  layer  made  of  al-
lochemical-sparry  limestone  (Fig. 5).  All  the  types  of  car-
bonate  rocks  contain  concretionary  cherts  in  the  form  of
lumps, lenses and concretionary interlayers (Fig. 3).

In the lower part of the column, within the sequence of

marly limestone, there is an association of sediments, which,
according to all its characteristics, corresponds to primary
pyroclastic material. The association is composed of a lami-
na (1 mm) made of crystalloclasts (crystalloclastic tuff) and
a layer of clay (10 cm) (Fig. 6).

Fig. 3.  Local  lithologi-
cal  column  of  a  part  of
the  Struganik  quarry,
western Serbia.

DJERIĆ, GERZINA, GAJIĆ and VASIĆ

Crystalloclasts of quartz, feldspars, and biotite are petro-

genetic  components  in  the  lamina  of  crystalloclastic  tuff.
Quartz  is  completely  transparent  (vitrified).  Quartz  grains
are  usually  broken.  Bipyramidal  grains,  which  undoubtedly
point to the volcanic origin, are present as well. Feldspars are
represented  by  transparent  sanidine  with  clearly  visible  fis-
sility  and  acid  to  intermediate  plagioclases  of  milky-white
colour. The most abundant coloured mineral is biotite.

Clay occurs in the form of a 10 cm thick layer which direct-

ly  overlies  the  lamina  of  crystalloclastic  tuff.  XRF  analyses
identified  three  crystal  phases.  Clay  minerals  of  the  smectite
group  prevail,  while  calcite  and  quartz  are  subordinate.  The
results of differential thermal and thermal gravimetric investi-
gations show that the clay is made of smectite and about 10 %
of calcite. The analysed smectite corresponds to Al-montmo-
rillonite with Ca and Mg, as interlayer cations, which was con-
firmed by chemical analyses (Table 1).

Fig. 4. Bouma sequence in allochemical-sparite: interval of parallel
lamination (b) and interval of wavy lamination (c), Struganik quar-
ry, western Serbia (photo V. Gajić).

Fig. 5. Paleodictyon structure in allochemical-sparry limestone,
Struganik quarry, western Serbia (photo V. Gajić).

Fig. 6. Upper Cretaceous layers in the Struganik quarry: A – Crys-
talloclastic tuff laminae; B – Smectite clay and C – Marly lime-
stone Struganik, western Serbia (photo V. Gajić).

Fig. 7. Microphotograph of 0.063—0.125 mm fraction separated
from smectite clay, Struganik quarry, western Serbia. A – Apatite;
R – Radiolarians; S – Spongi spicules, and C – Zircon.

Oxides Weight

SiО

48.67

ТiО

0.13

Аl

21.51

Fе

2.03

МnО *
МgО

4.16

CаО

4.27

Nа

0.05

2.09

CО

tr.

СО

tr.

Org. mat.

0.10

11.72

5.73

Sum. 100.46

Table 1: Chemical composition of smectite clay (fraction separated
minor off 5

µm) from the Struganik quarry section.

DJERIĆ, GERZINA, GAJIĆ and VASIĆ

Radiolarian dating

All the radiolarian specimens presented in this study were

obtained from a single clay sample (Figs. 3, 6). The produc-
tive  sample  212  is  from  grey,  soft  clay  and  it  was  treated
only  with  water.  The  clay  intercalations  of  carbonate  sedi-
ments  from  Struganik  contain  well  preserved  but  relatively
diverse  radiolarian  fauna.  Radiolarians  occur  together  with
abundant  sponge  spicule  fragments  and  sponge  carcasses.
The radiolarian fauna of sample 212 comprises (Fig. 8): Dic-
tyomitra formosa Squinabol, Dictyomitra koslovae Foreman,
Dictyomitra torquata Foreman, Alievium sp. cf. A. superbum
(Squinabol),  Pseudoaulophacus  sp.  cf.  P.  venadoensis  Pes-
sagno, Pseudoaulophacus sp. and Stichomitra sp.

According to Schaaf (1985) and Bandini et al. (2006) the

range  of  Dictyomitra  formosa  Squinabol  is  Late  Albian  to
Early  Campanian.  According  to  several  authors  (Nakaseko
& Nishimura 1981; Mizutani et al. 1982 and San Filippo &
Riedel  1985)  Dictyomitra  koslovae  Foreman  characterizes
the  interval  Santonian—Campanian.  However,  data  of  Vish-
nevskaya  (2001)  and  Deschamps  et  al.  (2000)  suggest  that
Dictyomitra koslovae Foreman indicates the interval Conia-
cian—Early Campanian. The presence of Dictyomitra torqua-
ta  Foreman  and  Pseudoaulophacus  sp.  cf.  P.  venadoensis
Pessagno,  confirms  that  the  fauna  cannot  be  younger  than
the  Early  Campanian  (O’Dogherty  1994;  Vishnevskaya
2001).  Ohmert  (2006)  suggested  that  Alievium  superbum
(Squinabol)  indicates  the  interval  Turonian  to  Coniacian,
sometimes  to  Santonian.  Therefore  the  age  of  the  fauna
could be assigned to Early Senonian.

This assemblage is similar to the Late Cretaceous assem-

blage of Romania (Vishnevskaya 2001), Great Caucasus
(Vishnevskaya 2001) and Nicoya Complex, Costa Rica (De-
nyer & Baumgartner 2006).

The radiolarian assemblage derived from a single sample,

thus the vertical distribution of radiolarian taxa in the section
could not be studied. Therefore, only basic data on these fos-
sils are presented here and they were used for new biostrati-
graphic interpretations.

Conclusions

When we talk about the environment of deposition of the

investigated rocks and marine sediments, there could be two
explanations. The first refers to the environment and condi-
tions of deposition of the autochthonous rocks in which the
lamina made of crystalloclastic tuff and the layer of clay are
found. The mechanism of inflow and deposition of pyroclas-
tic material should also be explained.

Autochthonous sediments are represented by marly lime-

stone and marlstone of micritic to biomicritic composition,
in which badly preserved radiolarians and silicisponges are
found. The presence of well-preserved silicisponge spicules
and radiolarians in clay should also be mentioned. The Early
Senonian age of the analysed clay is based on radiolarians.

Concretionary cherts indicate the presence of organogenic

siliceous remains. Such an association of rocks and fossils is
characteristic for a deep-marine sedimentation area. The dis-

tinct  predomination  of  silicisponge  spicules  over  radiolari-
ans in clay (noticed in carbonate sediments and particularly
in  clay)  points  to  a  moderately  deep-water  environment
(Vishnevskaya  1984).  A  finding  of  Paleodictyon  is  another
indicator  of  a  deep-water  environment,  to  the  boundary  of
bathyal-abyssal.  Presence  of  layers  of  allochemical-sparite,
calcarenite  and  calcirudite  with  the  characteristic  textures
from  the  Bouma  sequence  points  to  occasional  inflow  of
shallow-water  material  by  turbiditic  flows  along  the  conti-
nental slope, that is through the bathyal zone. According to
these data, it can be concluded that the Struganik Limestone
originated  in  a  deep-water  environment,  in  a  sedimentation
area on the continental slope.

The mineralogical characteristics of the crystalloclastic tuff

and clay show that the primary material was of volcanic origin
– the pyroclastic material, from which these sediments origi-
nated, was a product of acid-to-intermediary volcanism (quartz-
sanidine-plagioclase-biotite). The pyroclastic material is, for the
most part, made of fragments of volcanic glass (vitroclasts) with
some crystalloclasts (fragments, most probably of phenocrysts).
The largest crystalloclasts occur in the lamina made of crystal-
loclastic tuff, while smaller crystalloclasts are present in the lay-
er  of  clay  with  a  tendency  towards  upwardly  decreasing
grain-size. This fact is very important because it indicates that
the primary accumulated pyroclastic sediment was graded. Dif-
ferentiation of the pyroclastic material by size was gravitational,
that is the largest clasts were deposited first and accumulation of
finer clasts followed. A rather transparent pyroclastic cloud was
blown  by  wind  above  the  Upper  Cretaceous  Ocean.  Due  to
slower movement of the cloud, gravitationally differentiated fall
of clasts started and it continued through the aqueous environ-
ment  all  the  way  to  the  sedimentation  area  on  the  continental
slope where the material was eventually deposited as a graded
layer.  This  event  was  very  short  in  a  geological  sense  and  it
was  followed  by  sustained  deep-water  sedimentation.  In  an
early  phase  of  diagenesis,  fragments  of  volcanic  glass  were
transformed into clay minerals from the smectite group due to
reaction with the intergranular sea water. Geochemical charac-
teristics  of  the  environment  in  which  the  transformation  oc-
curred,  resulted  in  the  formation  of  montmorillonite  with  Ca
and Mg, as interlayer cations.

Acknowledgments: We wish to thank Prof. Valentina Vish-
nevskaya for her kind contributions during the preparation of
this paper. The authors gratefully acknowledge Ugur Kagan
Tekin and Jozef Michalík for their constructive comments on
the manuscript. The work was supported by the Serbian Min-
istry of Science and Technological Development (Projects
No. 146009 and 146013).

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