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Introduction
The Timok Eruptive Area (further: TEA) is situated in the
eastern Serbian Carpatho—Balkanides within the Getic tec-
tono-stratigraphic unit (Kräutner & Krstić 2003). Until recent-
ly, this area has been regarded as geotectonically part of the
Kučaj-Svrljig tectono-sedimentary zone within the Karpati-
kum (Andjelković 1978; Andjelković & Nikolić 1980).
Nowadays it is adjoined to the Kučaj terrane, one of the sev-
eral large Alpine geotectonic units of the eastern Serbian Car-
patho-Balkanides (Karamata & Krstić 1996). Berza et al.
(1998) regarded the TEA as part of the Banatitic Magmatic
and Metallogenetic Belt (BMMB), which represents a com-
plex calc-alkaline magmatic arc of Late Cretaceous age. The
TEA started its evolution with the Albian transgression, sedi-
mentation continued through the Cenomanian, and during Tu-
ronian it became a volcanic area (Djordjević & Banješević
1996). It comprises Turonian (—Coniacian) andesitic, Conia-
cian—Maastrichtian andesitic-basaltic volcanic rocks and
Campanian dioritic, quartz-dioritic and monzonitic plutonic
rocks (Milovanović et al. 2005). Although many articles have
been published on the petrology of the TEA and the wider
area (Divljan 1958; Drovenik et al. 1962; Nikolić & Andjelko-
vić 1967; Karamata et al. 1994, 1997; Djordjević &
Banješević 1996; Ciobanu et al. 2002; Heinrich 2002; Quadt
et al. 2002; Djordjević 2004—2005; Milovanović et al. 2005;
Upper Cretaceous volcanoclastic-sedimentary formations in
the Timok Eruptive Area (eastern Serbia): new
biostratigraphic data from planktonic foraminifera
DARIVOJKA LJUBOVIĆ-OBRADOVIĆ
1
, IVANA CAREVIĆ
2
, MONIKA MIRKOVIĆ
1
and NENAD PROTIĆ
1
1
Geological Institute of Serbia, Rovinjska St. 12, 11000 Belgrade, Serbia;
darivojka.lj.o.@gis.co.rs; monika.mirkovic@gis.co.rs; nenad.protic@gis.co.rs
2
Faculty of Geography, University of Belgrade, Studentski trg 3/3, 11000 Belgrade, Serbia; carevic.ivana@gmail.com
(Manuscript received November 3, 2010; accepted in revised form March 17, 2011)
Abstract: The biostratigraphy of the Upper Cretaceous volcanoclastic-sedimentary formations cropping out in the Timok
Eruptive Area of the eastern Serbian Carpatho-Balkanides is presented. Four lithostratigraphic units of formation rank are
recognized in the Timok area: Stublica Clastics (Upper Albian/Cenomanian), Oštrelj (Lower Turonian/Santonian), Bor
Clastics (Campanian/Maastrichtian) and Bukovo (Campanian/?Maastrichtian). Forty two species of planktonic foraminifera
have been determined in the studied area. Eight planktonic foraminiferal zones of Middle Cenomanian through Middle
Campanian age have been recognized. These are: Thalmanninella reicheli Interval Zone (Middle Cenomanian), Rotalipora
cushmani Taxon Range Zone (Upper Cenomanian), Helvetoglobotruncana helvetica Taxon Range Zone (Lower Turonian),
Marginotruncana sigali—Dicarinella primitiva Interval Zone (Upper Turonian to lowermost Coniacian), Dicarinella
concavata Interval Zone (Lower Coniacian to lowermost Santonian), Dicarinella asymetrica Taxon Range Zone (Santonian),
Globotruncanita elevata Interval Zone (Lower Campanian) and the Globotruncana ventricosa Interval Zone (Middle
Campanian). The scarcity or lack of zonal species in the Lower Cenomanian and Upper Campanian/Maastrichtian strata
prevents recognition of the nominal zones. The Upper Cretaceous planktonic foraminiferal zones from the Timok Eruptive
Area are correlated with coeval zones from adjacent regions of Bulgaria and Romania and from other Tethyan regions.
Key words: Upper Cretaceous, eastern Serbia, Timok Eruptive Area, biostratigraphy, volcanoclastic—sedimentary
formations, planktonic foraminifera.
Fig. 1. Location of studied sections within the Timok Eruptive
Area, eastern Serbia.
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Zimmerman et al. 2008; Banješević 2010) the stratigraphic set-
ting of the Upper Cretaceous formations has received very little
attention (Bogdanović 1965; Andjelković & Antonijević 1975;
Djajić & Pantić 1998). Up to now biostratigraphic characteris-
tics, as well as lithostratigraphy of the TEA have not been avail-
able. A preliminary report on the Timok group of formations is
given by Ljubović-Obradović (2010), and in her unpublished
PhD thesis (Ljubović-Obradović 2008) it includes the paleon-
tology and biostratigraphy of the Timok Eruptive Area.
The aim of this paper is to present Upper Cretaceous bios-
tratigraphic data and to propose a zonal scheme of the TEA
on the basis of planktonic foraminiferal associations. Eight
planktonic foraminiferal zones have been identified based on
the occurrence of index planktonic foraminifera. The occur-
rence and/or disappearance of some index microfossils were
used as references for separating these zones.
The study area is located between 22°18
’ to 22°00’E lon-
gitude and 44°06
’ to 43°45’N latitude (Fig. 1). Five well-
exposed stratigraphic sections of the Albian—Maastrichtian
strata were measured and sampled. The microfossil content
of the samples was studied in 76 thin-sections with an
optical microscope.
The thin-sections are housed in the collection at the Geo-
logical Institute of Serbia under inventory numbers which
are referred to in the text.
Stratigraphic background
Within the wider area of the studied section, the oldest
rocks are represented by Paleozoic conglomerates. They
consist of granitoid rocks and crystalline schists. Upwards
they are followed by sandstones, siltstones and claystones of
the same age (Veselinović et al. 1975). Sedimentation in the
Mesozoic started in the Jurassic transgressively over the old
basement. Within the framework of the Jurassic succession it
is possible to recognize all three ages: the Lower/Middle Ju-
rassic comprise clastic rocks and sandy limestones, while the
Upper Jurassic is built up of reef limestones (Djordjević &
Banješević 1997). They are unconformably overlain by Bar-
remian/Albian Urgonian limestones and sandstones. These
are followed by the Upper Cretaceous Timok Group of For-
mations described the text below. The Tertiary sedimentary
cover is composed mainly of Neogene lacustrine deposits.
Fig. 2. Lithological column and
biostratigraphy of the Lower Ap-
tian/Lower Turonian deposits in
the Stublica section. 1 – sandy
limestones; 2 – sandstones with
siderite; 3 – sandy claystones;
4 – sandy marlstones; 5 – sandy
siltstones; 6 – tuffs; 7 – breccias
with Fe concretions.
Stublica Clastics Formation
The Stublica Clastics Forma-
tion unconformably overlies the
Lower Aptian sandy limestones
with Palorbitolina lenticularis
and conformably underlies the
Oštrelj Formation (Fig. 2). It
was first described as Albian
“Lenovac Beds” by Andjelković
& Antonijević (1975). It is repre-
sented by sandstones with siderite
at the base dated as Late Albian
on the basis of ammonites.
It is transgressively overlain
by a continuous succession
with sandy claystones, sandy
marlstones and sandy siltstones
topped by sandstones with sid-
erite. The age of this unit is
dated as Cenomanian. It was
not possible to recognize the
Lower Cenomanian planktonic
foraminiferal zones due to the
lack of index species, but in the
upper part of the unit Thalman-
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ninella (the generic affiliation of the Albian-Cenomanian ro-
taliporids introduced in a recently published taxonomy by
González-Donoso et al. (2007) and Lipson-Benitah (2008) is
adopted in this study, although Gale et al. (2011) suspect that
the genus Thalmanninella may be polyphyletic) zonal spe-
cies Thalmanninella reicheli and Rotalipora zonal species
Rotalipora cushmani are identified suggesting a Middle and
Late Cenomanian age.
The formation thickness at the type section is inferred as
about 200 m. It attains a thickness of 241 m at Kravarnik,
but it is only 5 m thick at Gamzigrad.
Oštrelj Formation
The Oštrelj Formation was first recorded as a formal clastic
unit by Djordjević & Banješević (1997). This formation in-
cludes the succession from the Lower Turonian to Santonian. In
the section Zlot it conformably overlies the Stublica Clastics of
?Late Albian/Late Cenomanian age. It starts with the Lower Tu-
ronian (Helvetoglobotruncana helvetica Biozone) sandy lime-
stones and continues upwards with a rhythmic pattern of tuffs,
calcareous sandstones and marlstones (Fig. 3). The Upper Turo-
nian (Marginotruncana sigali—Dicarinella primitiva Biozone)
is represented by sandy limestones, calcareous sandstones, tuffs
and marlstones. Upwards it grades into Coniacian (Dicarinella
concavata Biozone) marlstones and tuffs. The upper part of the
formation also consists of marlstones and tuffs dated as Santo-
nian (Dicarinella asymetrica Biozone). The Oštrelj Formation’s
thickness in the Zlot locality reaches about 500 m.
In the type section Oštrelj, the formation is more calcare-
ous and less volcanogenic (Fig. 4). It consists of a 414 m
thick succession dominated by sandy limestones interbedded
with marly limestones and tuffs. The Late Turonian/Middle
Campanian age assignment of the Oštrelj Formation in the
type locality is based on planktonic foraminifera with five
biozones being recognized: Marginotruncana sigali—Dicari-
nella primitiva in the Upper Turonian to lowermost Conia-
cian; Dicarinella concavata in the Coniacian to lowermost
Santonian; Dicarinella asymetrica in the Santonian; Glo-
botruncanita elevata in the Lower Campanian and Glo-
botruncana ventricosa in the Middle Campanian.
The Oštrelj Formation can also be observed in the Viljor sec-
tion (Fig. 5). There it consists of a similar volcano-sedimentary
succession of Late Turonian/Santonian age rich in macrofos-
sils (bryozoans and echinoids)
with three planktonic foramin-
iferal biozones recognized (same
as previous). The Lower Turonian
(Helvetoglobotruncana
helvetica
Biozone) of the Oštrelj Formation
is missing in the Viljor section, but
is recorded in the Stublica section
conformably overlying the Stublica
Formation (Fig. 2).
Bor Clastics Formation
Petković (1931) was among the
first geologists to mention the pres-
ence of conglomerates in the TEA,
initially named the “Bor conglom-
erates” after the city of Bor. Subse-
quently, they were noticed by
Marić (1957) and described by
Divljan (1958). Their Senonian
age was proposed by Bogdanović
(1965). Recently, Ljubović-Obra-
dović (2008, 2010) introduced the
term Bor Clastics Formation for
the succession composed of a
mixture of clastic rocks represented
by conglomerates, various sand-
stones and claystones.
Fig. 3. Lithological column and bio-
stratigraphy of the Lower Aptian/San-
tonian deposits in the Zlot section.
1 – limestones; 2 – conglomerates;
3 – marlstones; 4 – aglomerates;
5 – sandy limestones; 6 – tuffs; 7 –
calcareous sandstones.
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The transition from the Oštrelj Formation to the Bor Clas-
tics Formation is well visible in the Viljor section (Fig. 5).
Above the sandstones the succession is dominated by con-
glomerates overlain again by sandstones with gastropod re-
mains. The age of this sequence is assigned to the
Campanian based on the occurrence of Globotruncana ven-
tricosa. The thickness is 80 m. It passes upward to a 30 m
thick Maastrichtian sandstone unit with intercalated layers of
claystones containing Gansserina gansseri. It is topped by
grey and yellow calcareous-clayey sandstones rich in well
preserved Maastrichtian spores and pollen (Djajić & Pantić
1998). The lack of Campanian/Maastrichtian zonal species
in the formation does not allow the nominal zones to be
recognized.
Bukovo Formation
In the Karaula-Bukovo section, the Bukovo Formation
(Ljubović-Obradović 2008, 2010) overlies the tuffites of the
Oštrelj Formation (Fig. 6). At the base, there are claystones
and marlstones overlain by sandy limestones with intercalat-
ed layers of claystones. Sandy limestones are rich in benthic
foraminifera, rudists bioclasts (e.g. Biradiolites, Radiolites),
gastropods, and corals. The following benthic foraminiferal
species known from Campanian age are determined: Orbi-
toides media, Orbitoides tissoti, Siderolites charentensis, Si-
derolites vidali and Vidalina hispanica. The age is also
supported by the index planktonic foraminiferal species Glo-
botruncanita elevata and Globotruncana ventricosa. This
sequence attains a thickness of about 90 m.
In the upper part the succession continues with pelagic
claystones and marlstones most probably dated as ?Maas-
trichtian on the basis of scarce planktonic foraminifera. The
thickness of this sequence reaches about 70 m.
Biostratigraphy of planktonic foraminifera in the TEA
Planktonic foraminifera are the main components in all mi-
crofossil assemblages in the investigated sediments. More
Fig. 4. Lithological col-
umn and biostratigraphy
of the Upper Turonian/
Middle Campanian depos-
its in the Oštrelj section.
1 – tuffs; 2 – sandy lime-
stones; 3 – marly lime-
stones; 4 – aglomerates.
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than forty planktonic species have been identified in the TEA.
The recognized biozones span the Middle Cenomanian to
Middle Campanian interval. The definitions of the biozones
are given following the latest concepts by Premoli Silva &
Verga (2004), Robaszynski et al. (2000), Robaszynski & Ca-
ron (1995), Premoli Silva & Sliter (1995), as well as Sliter
(1989) and Caron (1985). The correlation scheme between the
eastern Serbian Upper Cretaceous planktonic foraminiferal
zones with adjacent regions of Bulgaria and Romania as well
as the other Tethyan regions is given in Fig. 7.
Thalmanninella reicheli Interval Zone
D e f i n i t i o n : Biostratigraphic interval from the first oc-
currence of Thalmanninella reicheli to the first occurrence of
Rotalipora cushmani.
R e m a r k s : This zone is characterized by the presence of
Thalmanninella reicheli, Thalmanninella deeckei, Parathal-
manninella appenninica, Praeglobotruncana stephani and
Praeglobotruncana delrioensis.
Age and correlation: This zone corresponds to the Thal-
manninella reicheli Zone of Caron (1985), Sliter (1989),
Robaszynski & Caron (1995) and Premoli Silva & Verga (2004);
to the lower part of the Rotalipora cushmani Zone of Dimitrova
& Valchev (2007) and Peryt (1980); to the R. cushmani Zone of
Ion & Szasz (1994). The age of this zone is Middle Cenomanian.
D i s t r i b u t i o n : Stublica Clastics Formation (sections
Stublica and Zlot).
Rotalipora cushmani Taxon Range Zone
D e f i n i t i o n : Biostratigraphic interval represented by the
total range of Rotalipora cushmani.
Fig. 5. Lithological column and biostratigraphy of the Upper Turonian/Maastrichtian deposits in the Viljor section. 1 – tuffs; 2 – sandy
marlstones; 3 – sandy limestones; 4 – sandstones; 5 – claystones; 6 – conglomerates; 7 – bryozoans; 8 – echinoids; 9 – gastropods.
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R e m a r k s : The planktonic foraminiferal assemblage of
this zone includes Rotalipora cushmani, Thalmanninella
deeckei, Parathalmanninella appenninica and Praeglobotrun-
cana stephani.
A g e a n d c o r r e l a t i o n : This zone is the same as the
Rotalipora cushmani Zone recognized by Caron (1985),
Sliter (1989), Robaszynski & Caron (1995) and Premoli Silva
& Verga (2004). It corresponds to the upper part of the R.
cushmani Zone of Dimitrova & Valchev (2007) and Peryt
(1980); to the W. paradubia Zone and the lower part of the
D. imbricata Zone of Ion & Szasz (1994). The age of this
zone is Late Cenomanian.
D i s t r i b u t i o n : Stublica Clastics Formation (sections
Stublica and Zlot).
Helvetoglobotruncana helvetica Taxon Range Zone
D e f i n i t i o n : Biostratigraphic interval represented by the
total range of Helvetoglobotruncana helvetica.
R e m a r k s : The assemblage of this zone contains
Helvetoglobotruncana cf. helvetica and Praeglobotruncana
stephani present throughout this interval. Globotruncana
linneiana and Marginotruncana coronata first appeared in
the lower part of the interval. Representative species of the
upper part of this interval are Dicarinella algeriana, Dicari-
nella canaliculata, Dicarinella imbricata, Dicarinella
hagni,
Falsotruncana
maslakovae,
Marginotruncana
pseudolinneiana,
Marginotruncana
marginata
and
Whiteinella praehelvetica.
Age and correlation: This zone can be correlated with
the W. archeocretacea Zone and H. helvetica Zone in the
standard zonations (Caron 1985; Sliter 1989; Robaszynski &
Caron (1995); Premoli Silva & Verga 2004). It is identical
with the H. helvetica Zone of Peryt (1980). It corresponds to
the D. imbricata Zone and the lower part of the M. renzi—M.
sigali Zone of Dimitrova & Valchev (2007). The Helvetoglo-
botruncana helvetica Zone defined here is correlated with
the joint interval from the upper part of the D. imbricata Zone
to the lower part of M. sigali Zone of Ion & Szasz (1994). The
age of this zone is assigned to the Early Turonian.
D i s t r i b u t i o n : Oštrelj Formation (sections Stublica
and Zlot).
Marginotruncana sigali—Dicarinella primitiva Interval Zone
D e f i n i t i o n : Biostratigraphic interval between the last
occurrence of Helvetoglobotruncana helvetica and the first
occurrence of Dicarinella concavata.
R e m a r k s : The assemblage in this interval is character-
ized by the presence of Contusotruncana fornicata, Dicari-
Fig. 6. Lithological column and
biostratigraphy of the Campa-
nian/?Maastrichtian deposits in
the Karaula-Bukovo section.
1 – tuffites; 2 – claystones;
3 – marlstones; 4 – sandy
limestones; 5 – gastropods;
6 – rudists; 7 – corals.
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Fig. 7.
Proposed zonal scheme for the Upper Cretaceous succession in ea
stern Serbia compared with the zonations for Bulgaria, Romania,
Poland, eastern Iran and some important standard zo-
nations
of
the
Tethys.
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nella primitiva, Globotruncana bulloides, Marginotruncana
angusticarinata, Marginotruncana sigali, Dicarinella imbri-
cata, Dicarinella primitiva, Marginotruncana schneegansi,
Marginotruncana tarfayaensis, Dicarinella canaliculata,
Dicarinella cf. hagni, Marginotruncana angusticarinata,
Dicarinella canaliculata and Globotruncana lapparenti. All
of them appear for the first time in this zone. Other charac-
teristic species are Globotruncana linneiana, Marginotrun-
cana coronata and Marginotruncana marginata.
Fig. 8. Thin-section photomicrographs of the determined foraminifera from the Timok Eruptive Area. 1 – Contusotruncana fornicata (Plum-
mer), sample 69, Karaula-Bukovo section; 2 – Contusotruncana patelliformis (Gandolfi), sample 86, Karaula-Bukovo section; 3 – Contuso-
truncana patelliformis (Gandolfi), sample 83, Karaula-Bukovo section; 4 – Dicarinella cf. hagni (Scheibnerova), sample 1105, Viljor sec-
tion; 5 – Globotruncana arca (Cushman), sample 74, Karaula-Bukovo section; 6 – Dicarinella concavata (Brotzen), sample 465, Zlot
section; 7 – Dicarinella canaliculata (Reuss), sample 125, Viljor section; 8 – Gansserina gansseri Bolli, sample 345, Oštrelj section;
9 – Contusotruncana fornicata (Plummer), sample 339, Oštrelj section; 10 – Globotruncana bulloides Vogler, sample 69, Karaula-Bukovo
section; 11 – Globotruncanita conica (White), sample 90, Karaula-Bukovo section; 12 – Helvetoglobotruncana cf. helvetica (Bolli),
sample 176, Stublica section; 13 – Globotruncana rosetta (Carsey), sample 87, Karaula-Bukovo section; 14 – Globotruncana linneiana
(d’Orbigny), sample 87, Karaula-Bukovo section; 15 – Marginotruncana coronata (Bolli), sample 486, Zlot section; 16 – Globotruncana
hilli (Pessagno), sample 1058, Viljor section; 17 – Globotruncana arca (Cushman), sample 486, Zlot section; 18 – Gansserina sp., sam-
ple 1068, Viljor section. Scale bar = 100 µm.
A g e a n d c o r r e l a t i o n : The zone corresponds to the
joint interval from the upper part of the M. renzi—M. sigali
Zone to the lower part of the D. primitiva Zone of Dimitrova
& Valchev (2007); from the upper part of the M. sigali Zone
to the lower part of the M. tarfayensis Zone of Ion & Szasz
(1994). It corresponds to the lower part of the M. coronata
Zone of Peryt (1980); to the M. sigali Zone and the lowermost
part of D. concavata Zone of Babazadeh et al. (2007) and
Sliter (1989). This zone can be correlated with the M. sigali—
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Fig. 9. Thin-section photomicrographs of the determined foraminifera from the Timok Eruptive Area. 1 – Orbitoides tissoti Schlumberger,
sample 85, Karaula-Bukovo section; 2 – Marginotruncana pseudolinneiana Pessagno, sample 176, Stublica section; 3 – Palorbitolina len-
ticularis (Blumenbach), sample 703, Stublica section; 4 – Globotruncana cf. ventricosa White, sample 345, Oštrelj section; 5 – Orbitoides
media d’Archiac, sample 85, Karaula-Bukovo section; 6 – Globotruncana cf. ventricosa White, sample 344, Oštrelj section; 7 – Margino-
truncana sigali (Reichel), sample 461, Zlot section; 8 – Globotruncanita elevata (Brotzen), sample 342, Oštrelj section; 9 – Margin-
otruncana schneegansi (Sigal), sample 307, Oštrelj section; 10 – Praeglobotruncana delrioensis Plummer, sample 437, Zlot section;
11 – Dicarinella asymetrica (Sigal), sample 1022, Viljor section; 12 – Praeglobotruncana stephani (Gandolfi), sample 714, Stublica sec-
tion; 13 – Whiteinella praehelvetica (Trujillo), sample 176, Stublica section; 14 – Vidalina hispanica Schlumberger, sample 83, Karaula-
Bukovo section. For the figures 9.1, 9.3, and 9.5 scale bar = 200 µm, for all other figures scale bar = 100 µm.
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D. primitiva Zone of Premoli Silva & Verga (2004). The age
of this zone is Late Turonian to earliest Coniacian.
D i s t r i b u t i o n : Oštrelj Formation (sections Zlot, Oštrelj
and Viljor).
Dicarinella concavata Interval Zone
D e f i n i t i o n : Biostratigraphic interval between the first
occurrence of Dicarinella concavata and the first occurrence
of Dicarinella asymetrica.
R e m a r k s : The planktonic foraminiferal assemblage of
this zone includes Dicarinella concavata, Marginotruncana
marginata, Globotruncanita stuartiformis, Marginotruncana
angusticarinata, Marginotruncana coronata, Marginotrunca-
na marginata, Marginotruncana schneegansi, Marginotrun-
cana sigali, Globotruncana arca and Globotruncana bulloides.
Age and correlation: The D. concavata Zone corre-
sponds to the zone of the same name recognized by Sliter
(1989), Robaszynski & Caron (1995), Premoli Silva & Sliter
(1995), Robaszynski et al. (2000), Premoli Silva & Verga
(2004), Peryt (1980) and Babazadeh et al. (2007). It corre-
sponds to the upper part of the D. primitiva Zone and the D.
concavata Zone of Dimitrova & Valchev (2007); to the joint
interval from the upper part of the M. tarfayensis Zone to the
lower part of the D. asymetrica Zone of Ion & Szasz (1994).
The age of this zone is Early Coniacian to earliest Santonian.
D i s t r i b u t i o n : Oštrelj Formation (sections Zlot, Oštrelj
and Viljor).
Dicarinella asymetrica Taxon Range Zone
D e f i n i t i o n : Biostratigraphic interval represented by the
total range of Dicarinella asymetrica.
R e m a r k s : The assemblage of this zone contains Dicari-
nella asymetrica, Contusotruncana fornicata, Globotrunca-
na arca, Globotruncana hilli, Globotruncana lapparenti,
Globotruncana linneiana, Marginotruncana coronata, Glo-
botruncana bulloides, Globotruncanita stuartiformis and
Marginotruncana angusticarinata.
Age and correlation: This zone is identical with the D.
asymetrica Zone of Dimitrova & Valchev (2007), Babaza-
deh et al. (2007), Robaszynski & Caron (1995), Premoli Sil-
va & Sliter (1995), Robaszynski et al. (2000) and Premoli
Silva & Verga (2004). It corresponds to the upper part of the
D. asymetrica Zone of Ion & Szasz (1994); to the upper part
of the G. lapparenti Zone and C. fornicata Zone of Peryt
(1980); to the upper part of the C. fornicata Zone and to the
uppermost part of the D. concavata Zone and D. asymetrica
Zone of Sliter (1989). The age of this zone is Santonian.
D i s t r i b u t i o n : Oštrelj Formation (sections Zlot, Oštrelj
and Viljor).
Globotruncanita elevata Interval Zone
D e f i n i t i o n : Biostratigraphic interval between the last
occurrence of Dicarinella asymetrica and the first occur-
rence of Globotruncana ventricosa.
R e m a r k s : The last occurrence of Globotruncana bul-
loides, Globotruncanita stuartiformis and Marginotruncana
angusticarinata comprise the lower part of the zone.
Globotruncanita stuarti first appears in the upper part of the
zone. Contusotruncana fornicata, Globotruncana arca,
Globotruncana hilli, Globotruncana lapparenti, Globotrun-
cana linneiana and Globotruncanita elevata are common
throughout this interval.
Age and correlation: This zone corresponds to the
widely recognized Tethyan Globotruncanita elevata Interval
Zone (Caron 1985; Sliter 1989; Robaszynski & Caron
(1995); Premoli Silva & Sliter (1995); Babazadeh et al.
2007); to the lower part of G. elevata Zone of Dimitrova &
Valchev (2007) and Ion & Szasz (1994); to the lower part of
G. arca Zone of Peryt (1980). Premoli Silva & Verga (2004)
recognized this zone in the lowermost Campanian. The age
of this zone is assigned to the Early Campanian.
D i s t r i b u t i o n : Oštrelj Formation (section Oštrelj).
Globotruncana ventricosa Interval Zone
D e f i n i t i o n : Biostratigraphic interval defined by the first
occurrence of Globotruncana ventricosa and the first occur-
rence of Radotruncana calcarata.
R e m a r k s : The common species are Globotruncana
ventricosa, Globotruncana arca, Globotruncanita stuarti
and Gansserina gansseri.
Age and correlation: The G. ventricosa Zone corre-
sponds to the zone of the same range of Sliter (1989), Premoli
Silva & Sliter (1995) and Robaszynski & Caron (1995); to
the G. calcarata, G. havanensis and G. aegyptiaca Zones of
Premoli Silva & Verga (2004); to the uppermost part of the
G. arca Zone and lowermost part of the G. multispinus Zone
of Peryt (1980); to the uppermost part of the G. elevata Zone
and G. rugosa Zone of Ion & Szasz (1994) and to the upper-
most part of the G. elevata Zone and the lower part of the
G. stuartiformis Zone of Dimitrova & Valchev (2007). The
age of this zone is assigned to the Middle Campanian.
D i s t r i b u t i o n : Oštrelj Formation (section Oštrelj).
Conclusion
The Upper Cretaceous succession of the Timok Eruptive
Area in eastern Serbia includes four formations from base to
top: Stublica Clastics, Oštrelj, Bor Clastics and Bukovo. De-
tailed investigations of the five measured stratigraphic sec-
tions have yielded new data to establish the Upper Cretaceous
planktonic foraminiferal biostratigraphy of the TEA.
The planktonic foraminiferal assemblages of eastern Serbia
belong to the northern Tethyan bioprovince characterized by
representatives of the genera Contusotruncana, Dicarinella,
Falsotruncana, Gansserina, Globotruncana, Globotruncanita,
Helvetoglobotruncana, Marginotruncana, Parathalman-
ninella, Praeglobotruncana, Radotruncana, Rotalipora,
Thalmanninella and Whiteinella. The stratigraphic range of
42 planktonic foraminiferal species identified in the studied
successions had allowed recognition of eight biozones cov-
ering the Middle Cenomanian/Middle Campanian interval.
These are: the Thalmanninella reicheli Interval Zone (Mid-
dle Cenomanian), Rotalipora cushmani Taxon Range Zone
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BIOSTRATIGRAPHIC DATA FROM UPPER CRETACEOUS FORMATIONS (EASTERN SERBIA)
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA
GEOLOGICA CARPATHICA, 2011, 62, 5, 435—446
(Upper Cenomanian), Helvetoglobotruncana helvetica Taxon
Range Zone (Lower Turonian), Marginotruncana sigali—
Dicarinella primitiva Interval Zone (Upper Turonian to lower-
most Coniacian), Dicarinella concavata Interval Zone (Lower
Coniacian to lowermost Santonian); Dicarinella asymetrica
Taxon Range Zone (Santonian), Globotruncanita elevata
Interval Zone (Lower Campanian) and the Globotruncana
ventricosa Interval Zone (Middle Campanian).
The main result of this study is the establishment of an
Upper Cretaceous biozonal scheme of the eastern Serbian
Carpatho-Balkanides that may serve as a basis for further
biostratigraphic zonations in the Carpathians. The high-di-
versity planktonic foraminiferal assemblages from the
Timok Eruptive Area of eastern Serbian Carpatho-Balkanides
reveal a strong similarity to the Tethyan (Mediterranean)
Realm (Robaszynski & Caron 1995). Correlation of the pro-
posed zonation for eastern Serbia highlights good correlation
of the stratigraphic distribution of the Helvetoglobotruncana
helvetica Taxon Range Zone (Lower Turonian) from Poland,
Dicarinella asymetrica Taxon Range Zone (Santonian) from
Bulgaria and eastern Iran and Globotruncanita elevata Inter-
val Zone (Lower Campanian) from eastern Iran.
Acknowledgments: The authors are grateful to the two re-
viewers, Maria Rose Petrizzo (Universit
a
degli Studi di Mi-
lano) and Michael A. Kaminski (King Fahd University of
Petroleum and Minerals (KFUPM)) for their constructive
comments and remarks which greatly improved this paper.
This work was supported by the Ministry of Science and
Technological Development of the Republic of Serbia.
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Planktonic foraminifera
Contusotruncana fornicata (Plummer); Figs. 8.1, 9
Contusotruncana patelliformis (Gandolfi); Fig. 8.2,3
Dicarinella algeriana (Caron)
Dicarinella asymetrica (Sigal); Fig. 9.11
Dicarinella canaliculata (Reuss); Fig. 8.7
Dicarinella concavata (Brotzen); Fig. 8.6
Dicarinella cf. hagni (Scheibnerova); Fig. 8.4
Dicarinella imbricata (Monrod)
Dicarinella primitiva (Dalbiez)
Falsotruncana maslakovae Caron
Gansserina gansseri Bolli; Fig. 8.8
Gansserina sp.; Fig. 8.18
Globotruncana arca (Cushman); Fig. 8.5,17
Globotruncana bulloides Vogler; Fig. 8.10
Globotruncana hilli (Pessagno); Fig. 8.16
Globotruncana insignis (Gandolfi)
Globotruncana lapparenti (Brotzen)
Globotruncana linneiana (d’Orbigny); Fig. 8.14
Globotruncana orientalis Ei-Naggar
Globotruncana rosetta (Carsey); Fig. 8.13
Globotruncana cf. ventricosa White; Figs. 9.6, 4
Globotruncanita conica (White); Fig. 8.11
Globotruncanita elevata (Brotzen); Fig. 9.8
Globotruncanita stuarti (de Lapparent)
Globotruncanita stuartiformis (Dalbiez)
Helvetoglobotruncana cf. helvetica (Bolli); Fig. 8.12
Marginotruncana angusticarinata (Gandolfi)
Marginotruncana coronata (Bolli); Fig. 8.15
Marginotruncana marginata (Reuss)
Marginotruncana pseudolinneiana Pessagno; Fig. 9.2
Marginotruncana schneegansi (Sigal); Fig. 9.9
Marginotruncana sigali (Reichel); Fig. 9.7
Marginotruncana tarfayaensis (Lehmann)
Parathalmanninella appenninica (Renz)
Praeglobotruncana delrioensis Plummer; Fig. 9.10
Praeglobotruncana stephani (Gandolfi); Fig. 9.12
Radotruncana calcarata (Cushman)
Radotruncana subspinosa (Pessagno)
Rotalipora cushmani (Morrow)
Thalmanninella deeckei (Francke)
Thalmanninella reicheli Mornod
Ticinella roberti (Gandolfi)
Whiteinella praehelvetica (Trujillo); Fig. 9.13
Benthic foraminifera
Orbitoides media d’Archiac; Fig. 9.5
Orbitoides tissoti Schlumberger; Fig. 9.1
Palorbitolina lenticularis (Blumenbach); Fig. 9.3
Siderolites charentensis (Neumann)
Siderolites vidali (Douvillé)
Vidalina hispanica Schlumberger; Fig. 9.14
Appendix
List of planktonic and benthic foraminifera species recognized in this study, arranged in alphabetical order. Selected species are illustrated
in Figs. 8—9.
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