GEOLOGICA CARPATHICA
, APRIL 2017, 68, 2, 130 – 146
doi: 10.1515/geoca-2017-0011
www.geologicacarpathica.com
The Campanian–Maastrichtian foraminiferal
biostratigraphy of the basement sediments from the southern
Pannonian Basin (Vojvodina, northern Serbia): implications
for the continuation of the Eastern Vardar and Sava zones
MILENA DUNČIĆ, IVAN DULIĆ, OLIVERA POPOV, GORAN BOGIĆEVIĆ and ALAN VRANJKOVIĆ
Petroleum Company of Serbia, Scientific and technological center NTC NISNaftagas LLC Novi Sad, Narodnog fronta 12,
21000 Novi Sad, Serbia; milena.duncic@nis.eu; ivan.dulic@nis.eu; olivera.popov@nis.eu; goran.bogicevic@nis.eu; alan.vranjkovic@nis.eu
(Manuscript received March 29, 2016; accepted in revised form November 30, 2016)
Abstract: Micropalaeontological and biostratigraphical studies included Campanian–Maastrichtian complexes from five
oil exploration wells drilled in northern Serbia (Vojvodina): the first is a carbonateclastic complex and second is
a complex containing ophiolites intercalated with hemipelagic and pelagic sediments. Within the studied complexes, rich
associations of planktonic and benthic foraminifera, calcareous nannoplankton, palynomorphs, as well as shallow and
deepwater fossil detritus were determined. The presence of relatively rich associations of planktonic foraminifera
allowed recognition of two biozones: the Globotruncana ventricosa Zone, observed in the sediments of the carbonate
clastic complex and the Gansserina gansseri Zone, observed in both complexes. Except biozones, based on documented
index species, for some units in both complexes, larger benthic foraminifera species had special biostratigraphical value,
and in some of them, the calcareous nannoplankton zones were recognized. The studied complexes represent deepwater
formations, generated in oceanic island arc and trough zones. The presence of limestones, which originate from destroyed
rudist reefs, is explained by transfer by means of gravitational transport mechanisms of shallowwater sediments to
deepwater depositional environments. In this paper, the results of more detailed biostratigraphical and palaeoecological
studies of foraminifera associations in Campanian–Maastrichtian complexes in Vojvodina are presented. Combined with
lithological studies, seven units were determined within the complexes. The obtained results are important as a part of
multidisciplinary, regional exploration of both complexes, generated in specific geological conditions, that today
constitute a part of the preNeogene basement complex in the southeastern part of the Pannonian Basin. The Campanian–
Maastrichtian carbonateclastic complex represents sedimentary cover of the Eastern Vardar Ophiolitic Unit, while the
ophiolites intercalated with hemipelagic and pelagic limestones belongs to the Sava Zone.
Keywords: Campanian–Maastrichtian, Vardar Zone, Vojvodina, biostratigraphy, palaeoecology, foraminifera.
Introduction
Among the Mesozoic rocks of Vojvodina (northern Serbia),
constituting a part of the preNeogene basement complex in
the southeastern part of the Pannonian Basin, Upper Creta
ceous formations have the widest distribution. They are repre
sented by Senonian sediments with volcanoclastic rocks of
andesite trachytic composition (Karadjordjevo Formation)
and flysch deposits — Torda Formation (Kemenci & Čanović
1987; Čanović & Kemenci 1988, 1999). Only in a few wells
diffe rent types of development of the Upper Cretaceous were
observed, such as deepwater clastites of Albian–Cenomanian
age, organogenicdetritic limestones of Late Turonian–Early
Senonian age or red pelagic Santonian limestones (Kemenci &
Čanović 1997). A particular development in terms of micro
palaeontological and lithological characteristics is observed in
the Campanian–Maastrichtian complexes, which are the
subject of study in this paper. A brief overview of the general
characteristics of these complexes has been given earlier
without considering any other aspects of their interpretation
(Dunčić & Bogićević 2008).
The investigated Campanian–Maastrichtian carbonate
clastic complex was encountered in several deep oil exploration
wells of the Banat area (Central and North Banat) in Vojvodina.
In this paper, all units in this complex, observed in three wells
(Fig. 1): Krajišnik Mesozoic1 (KrMz1), Sajan1 (Sa1) and
Medja3 (Mdj3). The Campanian–Maastrichtian ophiolites
intercalated with hemipelagic and pelagic sediments have
been identified in a few wells in the South Bačka area, and the
complete development for the studied complex is present in
two wells (Fig. 1): Srbobran sever1 (Srs1) and Vrbas grad
(Vbg1).
This paper presents the results of the latest micro
palaeontological studies of the Campanian–Maastrichtian
carbonateclastic complex and the next one containing
ophiolites intercalated with sediments from wells in Vojvodina,
with the aim of establishing a more precise biostratigraphical
division and palaeoecological interpretation of studied
complexes, as well as determining the units within them.
Biostratigraphical analysis has enabled recognition of two
biozones, based on relatively rich and varied associations of
planktonic foraminifera: Globotruncana ventricosa Interval
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Zone (Middle to Late Campanian), identified in the sediments
of the carbonateclastic complex (well KrMz1) and the
Gansserina gansseri Interval Zone (Latest Campanian–Early
Maastrichtian), observed in sediments of both complexes
(wells KrMz1, Mdj3 and Vbg1). In some sediment units
from both complexes the biozones were not recognized,
however, according to entire microfossil assemblages
(especially larger benthic foraminifera species Siderolites
vidali, S. charentensis and Bulbophragmium aequale), their
age was determined as Upper Campanian. In terms of
calcareous nannoplankton, within some of these units, the
zones CC21a – CC22 were identified.
The studied complexes can be micropalaeontologically
correlated with similar complexes, the development of which
is documented in adjacent regions of the Tethyan bioprovince.
The purpose of this paper is to give a better view of the
biostratigraphy of the Campanian–Maastrichtian complexes
from wells in Vojvodina, which would contribute to better
understanding of the geological history of the exploration area
and geodynamic events during the Campanian– Maastrichtian.
The results of recent micropalaeontological, biostrati
graphical, palaeoecological and lithological studies have
indicated that the studied carbonateclastic complex in North
and Central Banat can be very well correlated with the
corresponding sediments within the Eastern Vardar Ophiolitic
Unit, while the complex, characterized by ophiolites,
intercalated with hemipelagic and pelagic sediments from the
wells of South Bačka demonstrates analogies with similar
units of the Sava Zone.
Geological setting
PreNeogene basement complex in the southeastern part of
the Pannonian Basin in Vojvodina consists of tectono
stratigraphic zones of five geotectonic units (Fig. 1). The
northern part of Vojvodina belongs to the Tisza Megaunit,
represented by a ProterozoicPalaeozoic granitemetamorphic
complex and Mesozoic formations, corresponding to the
Triassic age (Kemenci & Čanović 1997). The Eastern Vardar
Ophiolitic Unit and Sava Zone
cover the southern part of
Vojvodina. The south eastern
most part of Vojvodina belongs
to the SerbianMacedonian
Massif. The Jadar Block
involves the southwesternmost
part of Vojvodina, also
comprising adjacent areas of
northwest Serbia and northeast
Bosnia and Herzegovina.
The Mesozoic formations of
the Eastern Vardar Ophiolitic
Zone (Main Vardar Zone) can
be tracked from Transylvania
and the South Apuseni
Mountains to the north (Schmid
et al. 2008), across Vojvodina,
where they have been observed
in the preNeogene basement
complex in the Pannonian
Basin (Kemenci & Čanović
1997; Čanović & Kemenci
1999), stretching fur ther south
wards through east Serbia and
Macedonia (Kara mata et al.
1997; Schmid et al. 2008;
Robertson et al. 2009). Forma
tions corresponding to the
Eastern Vardar Ophiolitic Unit
were drilled in over 200 oil and
gas wells in the Vojvodina area.
The oldest Mesozoic formations
are repre sented by Jurassic
schistes lustres, while the most
striking Jurassic formations are
Fig. 1. Simplified and modified geotectonic map with positions of the studied wells in Vojvodina region
of northern Serbia (geo tectonic regionalization modified after Schmid et al. 2008).
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, 2017, 68, 2, 130 – 146
ophio lites and ophiolite mélange. The sedimentary cover com
pri sing Late Jurassic–Early Creta ceous and Late Cretaceous
units is developed trans gressively and discordantly over
Jurassic ophiolites and trench deposits. Within the Late
Jurassic–Early Cretaceous the following formations stand out:
pelagic limestones and marlstones of Tithonian–Valanginian
age and typically deepwater complexes of Tithonian–
Neocomian age, in some wells characterized by presence of
synsedimentary carbonated spilites (Čanović & Kemenci
1988). The Late Lower Cretaceous and Early Upper Cretaceous
are represented by Barremian–Aptian reef deposits of Urgonian
type, or deepwater sediments, followed by Aptian–Albian
clastites with notable turbidite features and deepwater clastic
carbonate sediments of Albian–Cenomanian age. Within the
Late Cretaceous, the Karadjordjevo Formation and Torda
Formation have the widest distribution.
According to numerous authors, the Sava Zone or Vardar
Zone Western Belt (Karamata et al. 2000, 2005; Robertson et
al. 2009) can be traced through southern and central Serbia in
the form of a narrow belt, which widens in the outskirts of
Belgrade and Mt. Fruška Gora and bends northwestward,
going further through northern BosniaHerzegovina and
Croatia (Robertson et al. 2009). The Sava Zone represents the
final suture collision zone between the Tisza and Dacia Mega
unit and the Dinarides (Schmid et al. 2008; Robertson et al.
2009), as the extension of the Periadriatic Zone (Pamić 2002).
In its northern part, this zone is usually limited to isolated
inselbergs within Cenozoic sediments (Robertson et al. 2009),
consisting of Upper Cretaceous ophiolites intercalated with
pelagic limestones, trench deposits, flysch, magmatic and
metamorphic rocks (Ustaszewski et al. 2010).
Material and methods
Using micropalaeontological methods of studying
foraminifera, rock samples from Campanian–Maastrichtian
complexes from five deep oil exploration wells in Vojvodina
area have been analysed. Analyses included core samples and
cuttings. Studies were performed using two methods: washed
residues and thin sections method. Foraminifera studies were
based on analysing 130 washed residues from cuttings and
cores and 180 thin sections from cores. Samples for the washed
residues analysis were usually prepared following the classic
micropalaeontological method. Micropalaeontological and
petrological thin section preparation was also carried out
according to standard procedure.
In semiquantitative analysis of foraminifera both thin
sections and washed residues were used. Semiquantitative
analysis included determination of relative abundance of
planktonic and benthic foraminifera, then agglutinated and
calcareous benthic foraminifera taxa, as well as other fossil
remains, present in studied sediments (microplankton of
calcisphaere type, detritus of shallow or deepwater fossils).
The obtained results were used for palaeoecological
interpretation. The results of these analyses, performed on
each sample, were presented within stratigraphic well sections,
using StrataBugs software (Figs. 2– 6). The relative abundance
of foraminiferal and other taxa is shown in four categories:
rare (<5 %), few (5 –10 %), common (10 –25 %) and abundant
(>25 % of whole microfossil assemblages).
All core and cutting samples, thin sections and micro
faunal foraminifera specimens are stored in NTC NIS
Naftagas LLC Novi Sad (collections of Regional geology
and unconventional resource department and Central
Laboratory Upstream).
Results
Among the studied Campanian–Maastrichtian complexes in
Vojvodina, development of seven units was observed, based
on the results of micropalaeontological, biostratigraphical and
lithological studies. Five units were determined in the
stratigraphic line of the carbonateclastic complex of Middle
Campanian–Lower Maastrichtian age from three wells in the
Banat area (Figs. 2–4), and two units within the complex
characterized by ophiolites intercalated with hemipelagic and
pelagic sediments of Upper Campanian–Lower Maastrichtian
age from two wells in the Bačka area (Figs. 5–6). While
defining the units, the data obtained by earlier micro
palaeontological and petrological studies were also used
(Kemenci & Čanović 1997), as well as the results of well log
data interpretation and correlation (unpublished NTC NIS
Naftagas LLC Novi Sad inhouse data).
Interpreted units of the investigated Campanian–Maastrich-
tian carbonate-clastic complex of the Central and North
Banat area
The limestones from destroyed reefs of the Middle-Late
Campanian (unit 1)
The limestones of destroyed reefs of MiddleLate
Campanian (unit 1) are determined in well KrMz1, depth
interval 3019–2939 m. This unit is in tectonic contact with
Albian–Cenomanian deepwater clastites, which have been
drilled in its basement, and underlies the following unit of this
complex (Fig. 2).
The unit consists of sandy biosparites and biosparudites
(Grainstone and Rudstone microfacies) and microconglo
meratic calcareous breccias. Fossil content in limestones is
represented by very small detritus of shallowwater fossil:
rudists (inner lamellar radiolitids layer, hippuritids fragments)
and other bivalve shells, serpulid tubeworms and calcareous
algae Coralinales. The age of unit 1 is indicated by the fact
that the studied sediments in well section conformably underlie
the next unit 2, the age of which was determined as Middle to
Late Campanian, based on foraminiferal data. These
limestones with reeffossil detritus were formed from
redeposited rudist reefs, transported into deeper depositional
environments.
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Fig. 2.
Stratigraphic column of the Krajišnik Mesozoic
1 (KrMz
1) well with distribution and relative abundance of foraminifera and shallow
water fossils detritus.
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The hemipelagic limestones of the Middle-Late Campanian
and Late Campanian (unit 2)
The hemipelagic limestones of the MiddleLate Campanian
and Late Campanian (unit 2) have also been determined in the
well KrMz1, depth interval 2939–2780 m (Fig. 2). Sediments
of this unit conformably overlie unit 1 and underlie unit 4 of
the carbonateclastic complex.
These sediments are represented by lightgrey to darkgrey
slightly sandy biointramicrites and biomicrites (Mudstone
Wackstone microfacies), interchanging with silty biointra
micrites (Wackstone microfacies). In the higher parts of the
unit (interval 2792–2780 m) these limestones contain
centimetre to decimetresized fragments of conglomeratic
biointrasparites (GrainstoneRudstone microfacies). Based on
the determined globotruncanid association, in biointramicrite
and biomicrite limestones of this unit in interval 2939–2792 m
Globotruncana ventricosa Interval Zone (MiddleLate
Campanian) was recognized. The Late Campanian age of the
sandy and silty biointramicrites and conglomeratic biointra
sparites of the higher part of unit 2 (interval 2792–2780 m),
was based on the entire microfossil assemblage or selected
taxa, among which a special biostratigraphical value is given
to the globotruncanid species Globotruncanita elevata and
larger benthic foraminifera species Siderolites vidali and
S. harentensis.
The coarse-grained clastites and limestones of destroyed
reefs from the Late Campanian (unit 3)
The coarsegrained clastites and limestones of destroyed
reefs from the Late Campanian (unit 3) are determined in the
well Sa1, depth interval 2415–2349 m (Fig. 3). Sediments of
this unit are in tectonic contact with Proterozoic–Palaeozoic
mylonite metamorphites of the Tisza Megaunit.
The lower part of unit 3 consists of coarsegrained clastites
(interval 2415–2380 m), represented by interbedding of sub
arkoses and siltstones with conglomeratic arkose. Presence of
microfauna was not registered in the studied coarsegrained
clastites, but a Late Cretaceous palynomorph association
(angiosperms from the Normapolles group) was identified.
The studied sediments most probably correspond to the
Upper Campanian, for in the well section, they underlie the
limestones, the age of which was determined as Upper
Campanian, according to foraminiferal data. The upper
part of unit 3 consists of limestones from destroyed
reefs (depth interval 2380–2349 m). These are lightgrey
biosparites to sandy biosparites (GrainstonePackstone
microfacies) and darkgrey biomicrites (PackstoneFloatstone
microfacies). The Late Campanian age of the upper part of
unit 3 was determined based on larger benthic foraminifera
species.
The presence of Late Campanian alodapic limestones in
deepwater complex, with reeffossil detritus, larger calcareous
benthic foraminifera of deeper parts of the euphotic zone, as
well as typical deepwater agglutinated benthic foraminifera,
is explained by transportation of material from shallowwater
environments into deeper parts of the basin.
The pelagic limestones from the Latest Campanian–Early
Maastrichtian (unit 4)
The pelagic limestones from the Latest Campanian–Early
Maastrichtian were distinguished as unit 4, determined in well
KrMz1, depth interval 2780–2624 m (Fig. 2). Sediments of
this unit conformably overlie the deposits of the older unit 2.
Unit 4 consists of silty biointramicrites (Wackestone
microfacies), containing numerous fault mirrors. The
Gansserina gansseri Interval Zone (Latest Campanian–Early
Maastrichtian) was recognized in the studied pelagic
limestones on the basis of globotruncanids. The Campanian–
Maastrichtian age of limestone was also confirmed based on
the identified palynomorph association, represented by a rich
association of fern spores and angiosperms belonging to the
Normapolles group as well as remains of marine phytoplankton
(algae Dinoflagellata).
The pelagic laminated limestones from the Early
Maastrichtian (unit 5)
The pelagic laminated limestones from the Early
Maastrichtian have been determined in well Mdj3, depth
interval 1738.1–1732 m (Fig. 4). The basement to the sediments
of this unit is unknown, for exploration drilling was terminated
in these deposits.
This unit is represented by laminar interbedding of grey
green biomicrites and sandy limestones with grey marly
siltstones. According to Čanović & Kemenci (1988), these
sediments were defined as a specific type of pelagic limestone,
corresponding to Late Maastrichtian. On the basis of the
newer micropalaeontological and biostratigraphical studies,
Gansserina gansseri Interval Zone was recognized in sediments
of this unit, most likely the uppermost part of this zone,
belonging to the Early Maastrichtian.
Interpreted units of investigated Campanian–Maastrichtian
complex containing ophiolites intercalated with hemipelagic
and pelagic sediments of the Southern Bačka area
The hemipelagic carbonates and clastites from the Late
Campanian with basic volcanites and their tuffs (unit I)
Unit I is determined in well Srs1, depth interval 2105–
1826 m (Fig. 5). The rocks which belong to this unit are in
tectonic contact with ProterozoicPalaeozoic metamorphites
of the Tisza Megaunit.
The sediments in the lower and middle part of unit (interval
2105–1905 m) are represented by darkgrey and whitish
coarsegrained calcareous sandstones with sandy limestone
boulders, finegrained sandstones, laminated siltyclayey
marls and lightgrey biointrasparites (Packstone microfacies).
The upper part of the unit (interval 1905–1826 m) consists of
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Fig. 3. Stratigraphic column of the Sajan1 (Sa1) well with distribution and relative abundance of foraminifera and shallowwater fossils
detritus.
Fig. 4. Stratigraphic column of the Medja3 (Mdj3)
well with distribution and relative abundance of
foraminifera.
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darkgrey laminated sandy marls and sandstones, while the
highest levels consist of ferrouscalcareous sandstones and
sandy limestones. The main feature of this unit is that the
sediments in the lower and middle part alternate with basic
volcanites (diabases, spilites, pyroclastic breccia) and derived
tuffs (synchronous multiphase submarine ultrabasic
volcanism). The determined microfossil assemblage or
biostratigraphically significant globotruncanid species and
larger benthic foraminifera species indicate that the studied
unit corresponds to the Late Campanian. Nannozones were
also recognized in the sediments of the upper part of the unit
CC21a–CC22.
The pyroclastic breccia interbedded with pelagic limestones
from the Latest Campanian-Early Maastrichtian (unit II)
Unit II is determined in well Vbg1, depth interval 2500–
1885 m (Fig. 6). The well was terminated in pyroclastic
breccias, so that their basement in this well is unknown.
The pyroclastic breccias are composed of millimetre to
centimetresized angular fragments of diabases, spilites,
rhyolites and vitroclastic tuffs. Rock fragments are usually
melded together, less frequently cemented with tuffitic matrix
(devitrified, zeolitized, volcanic glass). In a number of separate
intervals (2100–2059 m, 1995–1975 m and 1905–1885 m)
pyroclastic breccias are intrastratified with intercalations of
brownishred and greygreen pelagic biomicrites (Wackstone
microfacies). The Gansserina gansseri Interval Zone was
recognized in the studied biomicrites on the basis of the
identified globotruncanid association.
Biostratigraphical comments
In the studied sediments of some units, two planktonic
foraminiferal zones have been recognized, based on the first
and last occurrence of the index taxa: Globotruncana ventricosa
Interval Zone and Gansserina gansseri Interval Zone.
The biostratigraphy of the Late Campanian units is based on
entire microfossil assemblages, which are grouped in three
types of foraminiferal assemblage.
The biostratigraphical distributions of selected planktonic
and benthic foraminiferal species from the studied area and
other Tethyan regions are shown in Fig. 7. In this paper,
the zonal scheme of planktonic foraminifera according
to Premoli Silva & Verga (2004) was adopted, for it
represents the synthesis of numerous zone schemes, which
were distinguished for different tropicalsubtropical palaeo
geographic areas.
Notable considerations on the differences in chrono
stratigraphic position of a certain zonal species of planktonic
foraminifera were given in the paper Kędzierski et al. (2015).
Emphasizing that far more precise bio strati graphic data could
be obtained by integrating the results of a number of different
methods, such as palaeomagnetostratigraphy and bio
stratigraphy based on different fossil groups, the authors
indicated the existance of the problem of diachronicity of the
first and the last occurrence of zonal species, caused by palaeo
environmental conditions in different bioprovinces.
Globotruncana ventricosa Interval Zone
Age: Middle to Late Campanian (Premoli Silva & Verga 2004).
Distribution: KrMz1 well — hemipelagic limestones of
MiddleLate Campanian (lower and middle part of unit 2),
depth interval 2939–2792 m (Fig. 2).
Assemblage: The lower boundary of Globotruncana
ventricosa Zone corresponds to the first occurrence of the
zonal marker, while the upper boundary is assumed below
the first occurrence of the species Gansserina gansseri and
larger benthic foraminifera species Siderolites vidali and
S. charentensis (Fig. 2).
The planktonic foraminifera are most abundantly represented
by: Contusotruncana fornicata, Globotruncana arca,
G. bulloides, G. hilli, G. lapparenti, G. linneiana and
G. orientalis. Small, simple morphotypes of planktonic
foraminifera (rstrategists) are also present, represented by
hedbergellids and biserial heterohelicids. The zonal species
Globotruncana ventricosa is shown in Figures 8 and 9.
The identified planktonic foraminifera are dominated by
keeled forms of complex (Kstrategists) morphotypes, as
specialized forms of planktonic foraminifera. They are typical
for oligotrophic environmental conditions and indicate good
stratification of the water column in tropical and subtropical
environments (Petrizzo 2002). These keeled planktonic
foraminifera represent the bathypelagic group (Caron &
Homewood 1983; Gasiński et al. 1999).
Among benthic foraminifera, agglutinated taxa
(Arenobulimina preslii, Bathysiphon sp., Dorothia pupa,
Marssonella trochus and Minouxia sp.) and calcareous taxa
(Bolivina sp., Gavelinella voltziana, Lenticulina sp. and
Lagenidae) were identified. The determined forms of
agglutinated benthic foraminifera belong to deepwater forms
and include mixed types (upper and middle to lower bathyal
zone). Outer shelf to upper bathyal environments are
characterized by specimens of Gavelinella (Hradecká et al.
1999). On the other hand, specimens of lagenids, and
specimens of Bolivina and Lenticulina are associated with
inner, middle or outer shelf to bathyal environments (Olsson &
Nyong 1984; Murray 1991). These are rarely present in the
studied foraminifera associations.
Remarks: The Globotruncana ventricosa Zone, recognized
in the studied area, corresponds to the zone of the same range
of Premoli Silva & Verga (2004). Based on regional and global
comparative study of planktonic foraminifera, Petrizzo et al.
(2011) indicated the variations of the first occurrence of
G. ventricosa across latitudes and the difficulties in using this
species as a zonal marker in tropical and subtropical low
latitude areas. Instead of G. ventricosa species, the authors
pointed out that first occurrence of species Contusotruncana
plummerae is a reliable bioevent and singled out this species
as a zonal marker in tropical and subtropical areas.
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Fig.
5.
Stratigrap
hic
column
of
the
Srbobran
sever
1
(Srs
1)
well
with
distributio
n
and relative abundance of foraminifera and detritus of shallow
water fossils.
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The Contusotruncana plummerae Zone is determined as the
stratigraphic interval between the lowest occurrence of this
species and the lowest occurrence of species R. calcarata.
Ogg & Hinnov (2012), while determining the age of
epoch / series and age / stage boundaries of the Cretaceous,
among other things, stated the planktonic foraminiferal
biozones, which were determined as composite according to
numerous authors. The Contusotruncana plummerae Zone
was distinguished in the MiddleUpper Campanian (Fig. 7).
Types of foraminiferal assemblage from the Late Campanian
The first foraminiferal assemblage in the Late
Campanian sediments characterizes the higher part of unit 2
Fig. 6.
Stratigraphic column of the
V
rbas grad
1 (Vbg
1) well with distribution and relative abundance of foraminifera, microplankton and detritus of inoceramids.
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in the well KrMz1, interval 2792–2780 m. Foraminiferal
association comprises planktonic, calcareous and agglutinated
benthic foraminifera, among which larger benthic foraminifera
forms predominate. Among other fossil remnants, the presence
of shallowwater fossil detritus is notable (Fig. 2). The keeled
planktonic foraminifera as well as most of the benthic
foraminifera indicate a deepwater character of the studied
unit. Besides them, shallowwater foraminifera, represented
by specimens of Siderolites have also been identified in the
studied unit. These are characteristic for deeper parts of the
euphotic zone in open shelves (Gušić & Jelaska 1990). Very
rich and diverse biodetritus originates mainly from rudists
(radiolitids, hippuritids), ostreids and other bivalve shells,
while echinoid spines, serpulid tubeworms and calcareous
Fig. 7.
C
orrelation scheme of biostratigraphical distribution of selected planktonic and benthic foraminifera species from studied area and other
Tethyan regions.
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algae Coralinales and Dasycladales detritus are also present.
Their presence in the studied sediments indicates the existence
of reef environments during the Late Campanian.
For determination of the Late Campanian age of the studied
sediments, globotruncanids bear a special biostratigraphical
value, above all the species Globotruncanita elevata, larger
benthic foraminifera species Siderolites vidali and
S. charentensis, as well as some other benthic foraminifera
species, such as Reussella szajnochae and Stensioeina
pommerana (Fig. 7).
The second foraminiferal assemblage in the Late
Campanian sediments is characteristic for the upper part of
unit 3 in the well Sa1, interval 2380–2349 m (Fig. 3).
Planktonic foraminifera species are not present in the
foraminiferal association, while larger benthic foraminifera
taxa dominate among the benthic foraminifera. Nevertheless,
shallowwater fossil detritus is the most frequent within the
microfossil association. Larger benthic foraminifer taxa
consist of: Goupillaudina sp., Pararotalia sp., Siderolites
charentensis, Siderolites vidali, as well as rotaliids. Other
identified benthic foraminifera are Gaudryina pyramidata,
Marssonella trochus (agglutinated benthic foraminifera) and
Gavelinella sp. (calcareous benthic foraminifera), which are
characteristic for outer shelf to upper bathyal environments.
Shallowwater fossil detritus comprises: bivalves (rudist
fragments – radiolitids, hippuritids predominate), echinoid
spines, bryozoans and calcareous algae Coralinales and
Dasycladales. Some species of benthic foraminifera from the
second foraminiferal assemblage are shown in Figure 10.
The third foraminiferal assemblage in Late Campanian
rocks is identified in hemipelagic carbonates and clastites of
the older unit I in the well Srs1 (Fig. 5). The diversity of
foraminiferal and other fossil assemblages and their relative
abundance change within the studied unit according to
lithological changes.
In coarsegrained calcareous sandstones in the lower part of
the unit larger benthic foraminifera (Goupillaudina sp.) and
deepwater agglutinated benthic foraminifera (Marssonella
trochus, Tritaxia sp. and Verneuilina sp.) are seldom present.
These sediments are characterized by detritus of different
shallowwater fossils (fragments of inner lamellar layers with
radiolitids and hippuritids shells, bryozoan fragments and
Fig. 8. SEM photomicrographs of the selected planktonic foraminifera from the third foraminiferal assemblage of Late Campanian rocks (1–7),
Globotruncana ventricosa Zone (8–9) and Gansserina gansseri Zone (10–11). 1–3 — Globotruncanita cf. atlantica Caron, Srs1, cutting
2095–2090 m; 4–5 — Globotruncana falsostuarti Sigal, Srs1, cutting 1985–1980 m; 6–7 — Contusotruncana fornicata (Plummer), Srs1,
cutting 1965–1960 m; 8–9 — Globotruncana ventricosa White, KrMz1, cutting 2825–2820 m and 10–11 — Globotruncanita elevata
(Brotzen), Vbg1, cutting 1985–1980 m.
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fragments of calcareous algae), which were transported from
shallower to deeper parts of the basin.
Planktonic and deepwater benthic foraminifera are present
in the foraminiferal association of finegrained sandstones and
laminated siltyclayey marls of the lower and middle part of
the unit (interval 2105–1905 m) (Fig. 5). Globotruncanids
comprise: Contusotruncana fornicata, Globotruncana arca,
G. bulloides, G. falsostuarti, G. linneiana, G. orientalis,
Globotruncanita cf. atlantica, Gl’ita elevata, Gl’ita stuarti
and Gl’ita stuartiformis. Apart from globotruncanids, the
opportunistic (rstrategists) morphotypes (epipelagic group)
are very seldom present. Agglutinated benthic foraminifera
are represented by: Arenobulimina preslii, Clavulinoides cf.
aspera, Dorothia pupa, Gaudryina pyramidata, Haplo-
phragmoides gr. walteri, Marssonella trochus, Tritaxia
tricarinata, Verneuilina tricarinata and simple tubular forms
Bathysiphon sp., Nothia sp. and Rhabdammina sp. Most of
these are characteristic for the upper bathyal zone, such as
specimens of Arenobulimina, Dorothia, Gaudryina, Mars-
sonella and Verneuilina (Olsson & Nyong 1984; Chacón et al.
2004). Some of them can also occur in lower bathyal
environments, such as specimens of Tritaxia (Olsson & Nyong
1984), and some among the identified representatives of
agglutinated foraminifera (Bathysiphon, Clavulinoides,
Dorothia, Gaudryina, Haplophragmoides, Marssonella,
Rhabdammina) are indicated as typical flyschtype
foraminiferal microfauna or typical for oceanic (abyssal)
environments (Kuhnt 1990; Kuhnt & Kaminski 1997). Deep
water calcareous benthic foraminifera consist of: Gavelinella
monterelensis, Gavelinella voltziana, Gyroidinoides nitidus,
Lenticulina sp., Neoflabellina suturalis and Stensioeina
pommerana. On the other hand, biointrasparites in the middle
Fig. 9. Thin section photomicrographs of the selected planktonic foraminifera from Globotruncana ventricosa Zone (1) and Gansserina gansseri
Zone (2–12). 1 — Globotruncana ventricosa White, KrMz1, core 2946–2937 m (I m); 2 — Globotruncanita stuarti (de Lapparent), KrMz1,
core 2664–2658 m (IV m); 3 — Globotruncanita cf. pettersi (Brotzen), Vbg1, core 2063–2059 m (II/15 m); 4 — Globotruncanita cf. conica
(White), Vbg1, core 2063–2059 m (II/15 m); 5 — Globotruncanita elevata (Brotzen), Vbg1, core 2063–2059 m (II m); 6 — Gansserina
gansseri (Bolli), Vbg1, core 2063–2059 m (I/10 m); 7 — Globotruncana aegyptiaca Nakkady, Vbg1, core 2063–2059 m (I m); 8 — Contuso-
truncana cf. walfischensis (Todd), Mdj3, core 1735,4–1732,8 m (II m); 9 — Globotruncana arca (Cushman), Mdj3, core 1735,4–1732,8 m
(II m); 10 — Globotruncana falsostuarti Sigal, Mdj3, core 1735,4–1732,8 m (II m); 11 — Contusotruncana patelliformis (Gandolfi), Mdj3,
core 1735,4–1732,8 m (I m); 12 – Globotruncanita cf. angulata (Tilev), Mdj3, core 1735,4–1732,8 m (I m).
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part of the unit are characterized by the presence of Siderolites
vidali.
Within the foraminiferal association in the laminated sandy
marls and sandstones of the upper part of the unit (interval
1905–1826 m) deepwater agglutinated benthic foraminifera
dominate. Calcareous benthic foraminifera taxa are also
present, while the planktonic foraminifera are seldom present
(Fig. 5). In the studied sediments, a rich association of
calcareous nannoplankton was determined: Arkhangelskiella
cymbiformis Vekshina, Calculites obscurus (Deflandre),
Eiffellithus eximius (Stover), Microrhabdulus decoratus
Deflandre, Micula concava (Strander), Micula decussata
Vekshina, Quadrum gothicum (Deflandre) etc. The main
feature of ferruginouscalcareous sandstones and sandy
limestones of the uppermost part of the unit is the presence of
larger agglutinated foraminifera Bulbophragmium aequale
and forms which belong to the family Labyrinthidomatidae
(Fig. 5).
Globotruncanid species Globotruncanita elevata, Gl’ita cf.
atlantica, Gl’ita stuarti and Globotruncana falsostuarti and
larger benthic foraminifera species Bulbophragmium aequale,
Siderolites charentensis and S. vidali had a great bio
stratigraphic value in determination of the Late Campanian
age of the studied sediments (Fig. 7). Within certain levels
of the upper part of the unit (samples of core 1902–1896 m),
CC21a–CC22 Nannozones were recognized. The selected
planktonic and benthic foraminifera from this foraminiferal
assemblage of Late Campanian rocks are shown in Figures 8,
10 and 11.
Gansserina gansseri Interval Zone
Age: Latest Campanian–Early Maastrichtian (Premoli Silva
& Verga 2004).
Distribution: KrMz1 well — unit 4, depth interval
2780–2624 m (Fig. 2), Mdj3 well — unit 5, depth interval
1738,1–1732 m (Fig. 4) and Vbg1 well — unit II, depth
interval 2500–1885 m (Fig. 6).
Assemblage: In the studied area this zone corresponds to
sediment units in which the species Gansserina gansseri is
constantly present (Figs. 2, 4 and 6). Planktonic foraminifera
are represented by: Archaeoglobigerina cf. cretacea, Contuso-
truncana fornicata, C. patelliformis, C. cf. walfischensis,
Globotruncana aegyptiaca, G. arca, G. bulloides,
G. falsostuarti, G. hilli, G. lapparenti, G. linneiana,
G. orientalis, G. ventricosa, Globotruncanita cf. angulata,
Gl’ita cf. conica, Gl’ita elevata, Gl’ita cf. pettersi, Gl’ita
stuarti, Gl’ita stuartiformis and Heterohelix globulosa.
Besides heterohelicids and archeoglobigerinids, other
rstrategists as well as r/K intermediate morphotype group are
present: hedbergelids, globigerinelloids and rugoglobigerinids.
Complex morphotypes (Kstrategists) represent the bathy
pelagic group. According to Abramovich et al. (2003), most of
them belong to subsurface or thermocline (even sub
thermocline) groups of foraminifera. The more Kselected of
the r/K intermediates are represented by trochospiral forms
with hemispheric small chambers and one peripheral keel, the
example of which is zonal species Gansserina gansseri.
Representatives of trochospiral genera Archaeoglobigerina
Fig. 10. Thin section photomicrographs of the selected benthic foraminifera from the second type foraminiferal assemblage of Late Campanian
sediments (1–4), the third type foraminiferal assemblage of Late Campanian rocks (5–6) and Gansserina gansseri Zone (7–8). 1 — Gaudryina
cf. pyramidata Cushman, Sa1; core 2353,2–2349,2 m (III m); 2 — Marssonella trochus (Orbigny), Sa1, core 2353,2–2349,2 m (II m);
3 — Pararotalia sp., Sa1, core 2379–2370 m (VII m); 4 — Siderolites charentensis, Sa1, core 2379–2370 m (I m); 5 — Siderolites vidali
Douvillé, Srs1, core 1844–1835 m (III/50 m); 6 — Goupillaudina sp., Srs1, core 2105–2096 m (IX/100 m); 7 — Reussella szajnochae
(Grzybowski), Vbg1, core 2063–2059 m (II m); 8 — Stensioeina pommerana Brotzen, Vbg1, core 2063–2059 m (II m).
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and Rugoglobigerina and planspiral genus Globigerinelloides
are some of the more rselected of the r/K intermediate
morphotype groups. Zonal marker Gansserina gansseri is
distinguished as a thermocline group foraminifera in the
Lower Maastrichtian, while unkeeled intermediate morpho
types belong to the subsurface water foraminifera group
(Abramovich et al. 2003). The species Heterohelix globulosa,
as an opportunistic taxon (rstrategists), also belongs to the
thermocline group of foraminifera.
Agglutinated benthic foraminifera have a deepwater
character (bathyal environments) and consist of: Arenobulimina
preslii, Bathysiphon sp., Caudammina cf. ovula, Dorothia
pupa, Gaudryina pyramidata, Haplophragmoides gr. walteri,
Marssonella trochus, Minouxia sp., Nothia sp., Rhabdammina
sp., Spiroplectinella sp., Tritaxia tricarinata and Verneuilina
tricarinata. Calcareous benthic foraminifera taxa are
represented by mixed forms: Bolivina sp., Gavelinella
monterelensis, Gavelinella voltziana, Gyroidinoides nitidus,
Lenticulina sp., Reussella szajnochae, Stensioeina pommerana
and forms from families Lagenidae, Miliolidae and
Nodosariidae. Other fossil remnants are represented by
microplankton (pithonellae and other calcisphaerae), which
are very rare in the studied pelagic units, and inoceramid detritus.
Biostratigraphical subdivision within a zone could be done
only for the sediments of unit 5 from Mdj3 well, based on the
presence of Contusotruncana cf. walfischensis species and
greater presence of rugoglobigerinids, characteristic of the
Maastrichtian sediments (Fig. 4). Considering all of this, the
studied sediments most probably correspond to the upper part
of the Gansserina gansseri Zone, of Early Maastrichtian age.
The selected planktonic and benthic foraminifera from the
Gansserina gansseri Zone are presented in Figs. 8–11.
Fig. 11. SEM photomicrographs of the selected benthic foraminifera from the third type foraminiferal assemblage of Late Campanian rocks
(1–11) and Gansserina gansseri Zone (12–13). 1 — Neoflabellina suturalis (Cushman), Srs1, cutting 1995–1990 m; 2 — Marssonella trochus
(Orbigny), Srs1, cutting 1985–1980 m; 3 — Gavelinella voltziana (d’Orbigny), Srs1, cutting 1980–1975 m; 4 — Tritaxia tricarinata (Reuss),
Srs1, cutting 1965–1960 m; 5 — Clavulinoides cf. aspera (Cushman), Srs1, cutting 1915–1910 m; 6 — Dorothia pupa (Reuss), Srs1, cutting
1915–1910 m; 7 — Gaudryina pyramidata Cushman, Srs1, cutting 1915–1910 m; 8 — Caudammina cf. ovula (Grzybowski), Srs1, cutting
1890–1885 m; 9 — Spiroplectinella cf. subhaeringensis (Grzybowski), Srs1, core 1844–1835 m (II m); 10 — Bulbophragmium aequale
Maync, Srs1, cutting 1855–1850 m;11 — Siderolites vidali Douvillé, Srs1, cutting 1835–1830 m; 12 – Arenobulimina preslii (Reuss),
KrMz1, cutting 2770–2765 m; 13 — Verneuilina tricarinata d’Orbigny, KrMz1, cutting 2755–2750 m.
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Remarks: The Gansserina gansseri Interval Zone,
recognized in the studied area, corresponds to the zone of the
same stratigraphic range of Premoli Silva & Verga (2004).
According to previous zonal schemes of planktonic
foraminifera the Gansserina gansseri Interval Zone was
attributed to the middle part of the Maastrichtian (Fleury 1980;
Robaszynski et al. 1984) or Late Maastrichtian (Caron 1985).
Later, after updating biozone boundaries according to the
results of palaeomagnetostratigraphic measurements, the
Gansserina gansseri Zone corresponded to the Latest
Campanian–Early Maastrichtian (Premoli Silva & Sliter 1995;
Robaszynski & Caron 1995; Premoli Silva & Verga 2004).
Ogg & Hinnov (2012) accepted the chronostratigraphical
position of this zone in the Latest Campanian–Earliest
Maastrichtian (Fig. 7).
Discussion
Micropalaeontological, biostratigraphical, palaeoeco
logical, as well as lithological studies of both complexes from
the wells in Vojvodina, indicated the development of a deep
trough during the Campanian–Maastrichtian age. The studied
complexes have a deepwater character and were most
probably formed in ocean island arc and trough zones.
Information on the deepwater character of the studied units
was obtained on the basis of relative abundance and diversity
of identified planktonic foraminifera (complex morphotypes
and the more Kselected of the r/K intermediates morphotypes)
and deepwater calcareous and agglutinated benthic
foraminifera. The carbonateclastic complex in Banat is
characterized by development of five units, which were
determined in three wells (Figs. 2–4). Their superposition
from the older towards the younger units indicates the process
of trough formation, deepening and creation of preconditions
for development of flysch formations. The other complex
characterized by ophiolites intercalating with hemipelagic and
pelagic deposits, was determined in two wells in South Bačka
and consists of two units (Figs. 5 and 6). It should be noted
that the studied Campanian–Maastrichtian complexes are in
tectonic contact with the older, deeper formations, such as
ProterozoicPalaeozoic granitemetamorphic complex of the
Tisza Megaunit (wells Sa1 and Srs1) or the Albian–
Cenomanian deepwater formation of the Vardar Zone (well
KrMz1). Up to now, the history of the trough’s development
and precise timing of its formation have not been clearly
defined.
Study of the palaeoecological characteristics of forami
nifera, as well as the lithological characteristics of the units of
both complexes, indicated that during the Campanian–
Maastrichtian, concurrently with deep trough development,
shallowwater areas where reefs were developed, also existed.
When it comes to the carbonateclastic complex in Banat, it is
indicated by the following determined units (Figs. 2 and 3):
limestones of destroyed reefs of MiddleLate Campanian age
(KrMz1 well) — unit 1, hemipelagic limestones of
MiddleLate and Late Campanian age (KrMz1 well) — unit 2
and coarsegrained clastites and limestones from destroyed
reefs of Late Campanian age (Sa1 well) — unit 3. When it
comes to the other complex, the existence of reef environments
during the Late Campanian is indicated by the development of
the older unit I from Srs1 well (Fig. 5). These units comprise
sandy biosparites, biosparudites, biomicrites, sandy and silty
biointramicrites with fragments of conglomeratic bio
intrasparites, microconglomeratic calcareous breccias, coarse
grained clastites, calcareous sandstones with fragments of
sandy rudist limestones, which occur within deepmarine
carbonateclastic sediments. The sediments of these units,
except for planktonic and deepwater benthic foraminifera, are
characterized by the presence of larger benthic foraminifera
(specimens of Siderolites, Pararotalia and Goupillaudina) as
well as other shallowwater fossils (rudist detritus and other
bivalve shells, serpulid tubeworms, echinoids, calcareous
algae and bryozoans), which indicate the existence of reef
environments in island arc zones during the Middle and Late
Campanian. The presence of limestones and other sediments
with reeffossil detritus in these deepwater complexes can be
associated with tectonically unstable conditions in the areas of
their generation, when the transfer of shallowwater rock and
fossil material from shallowwater to deepwater depositional
environments occurred by means of gravitational or other
transport mechanisms.
In the well Sa1 (Fig. 3) ProterozoicPalaeozoic meta
morphites of the Tisza Megaunit were drilled in the basement
of the studied deepwater carbonateclastic complex and the
two units are in tectonic contact. This indicates the presence of
large thrust systems, formed during the Palaeogene.
The studied complex, characterized by Campanian–
Maastrichtian ophiolites, intercalated with hemipelagic and
pelagic sediments from the wells Srs1 and Vbg1 (Figs. 5
and 6), can be very well correlated with similar formations
belonging to the Sava Zone. By its analogous palaeontological
and lithological characteristics, the studied complex of South
Bačka shows a connection with the prospects in NorthWest
Bosnia (northern parts of Mt. Kozara
—
Karamata et al. 2000,
2005) and East Croatia (Mt. Požeška Gora
—
Pamić & Šparica
1983). In the well Srs1 hemipelagic carbonates and clastites
in some levels interbed with diabases, spilites, their tuffs and
pyroclastic breccias, while in the well Vbg1 the red biomicrite
interbeds were determined in pyroclastic breccias. On the
northern slopes of Mt. Kozara (surroundings of Gornji
Podgradci village) and Mt. Požeška Gora (locality Nakop
stream) sediments that alternate with Late Cretaceous basalts
(pillow basalts and tuffs) are represented by red and grey
pelagic biomicrites and sandy limestones. Very rich
globotruncanid associations are characteristic of pelagic
limestones.
The Late Campanian–Early Maastrichtian age of the
ophiolites from the wells of South Bačka is documented on the
basis of micropalaeontological studies of the sediments which
interbed with basic volcanites and their tuffs. Documenting
the Late Cretaceous age of the ophiolites from South Bačka
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wells indicated that the dislocation of the blocks corresponding
to the Sava Zone extended more towards the north (Fig. 1),
compared to previous knowledge of their position (Schmid et
al. 2008). It is important to note that below the Campanian–
Maastrichtian ophiolites in the wells of South Bačka the Tisza
Megaunit metamorphites (well Srs1) were drilled, as is the
case with the Campanian–Maastrichtian carbonateclastic
complex in the well Sa1 in North Banat. Thus, in this case the
presence of remains of the large thrust systems in Late
Cretaceous formations in the southeastern part of the
Pannonian Basin can be assumed as well.
Conclusion
Both studied complexes have a deepwater character and
were most probably formed in ocean island arc and trough
zones. Significant information on the deepwater character of
studied units was obtained on the basis of relative abundance
and diversity of identified planktonic and benthic foraminifera
and analysis of their palaeobathymetrics.
The carbonateclastic complex of Banat is characterized by
five units: limestones from destroyed reefs of MiddleLate
Campanian age (KrMz1 well)
—
unit 1, hemipelagic limestones
from the MiddleLate and Late Campanian (KrMz1 well)
—
unit 2, coarsegrained clastites and limestones of destroyed
reefs from the Late Campanian (Sa1 well)
—
unit 3, pelagic
limestones of the Latest Campanian–Early Maastrichtian
(KrMz1 well)
—
unit 4 and pelagic laminated limestones of
the Early Maastrichtian (Mdj3 well)
—
unit 5. These units
represent blocks, which were defined in three wells, and
indicate the deepening trough where they were formed. The
complex, characterized by Late Cretaceous ophiolites
intercalated with hemipelagic and pelagic sediments of South
Bačka consists of two units: hemipelagic carbonates and
clastites of the Late Campanian with basic volcanites and their
tuffs (Srs1 well)
—
older unit I and pyroclastic breccia
interbedded with pelagic limestones of the Latest Campanian–
Early Maastrichtian (Vbg1 well)
—
younger unit II.
The studied complexes show analogous lithological and
palaeontological characteristics to Senonian pelagic and rudist
sediments from localities in the Vardar Zone, such as
Mt. Fruška Gora in Vojvodina (Dulić et al. 2004), Struganik
quarry in western Serbia (unpublished PhD thesis by Gajić,
2014), but also to sediments from some localities in the
CarpathoBalkanides, such as the complex Vrbovački reef in
eastern Serbia (SladićTrifunović 1992). Some units also
show characteristics analogous to the Senonian carbonate
formations in the Transdanubian Range Zone, such as the
Ugod Limestone and Polány Marl, typical bathyal Izsák Marl
Formation of the Mecsek Facies Unit within the Tisza Mega
unit (Haas et al. 2012), as well as Senonian, red pelagic
limestones of the Scaglia facies of the western Mediterranean
(Kuhnt 1990).
The complex characterized by Upper Cretaceous ophiolites
intercalated with hemipelagic and pelagic sediments can be
very well correlated with similar formations in other Sava
Zone localities, such as Mt. Požeška Gora or North Kozara
Mountain. This is important in terms of obtaining significant
data on the spatial distribution of blocks containing Late
Cretaceous ophiolites. There is an assumption of their presence
in several localities in Vojvodina, as well as in the wider
region, which certainly indicates a need for future studies of
the distribution of these blocks, in order to get as precise as
possible information about the process of final closure of the
Tethyan realm.
Acknowledgements: We would like to express our gratitude
to company NTC NISNaftagas LLC Novi Sad, for their
support and the possibility they provided to use unpublished
geological data from the exploration wells studied for the
purposes of this paper. We would like to express special grati
tude to Prof. Dr. M. Adam Gasiński for his constructive review
and suggestions as well as to the anonymous reviewer for the
critical review and useful comments. We also owe our grati
tude to Dr. Milan Kohút, Managing Editor of Geologica Car
pathica, who helped improving our paper by his suggestions
and proposals.
References
Abramovich S., Keller G., Stüben D. & Berner Z. 2003: Characterization
of Late Campanian and Maastrichtian planktonic foraminiferal
depth habitats and vital activities based on stable isotopes.
Palaeogeogr. Palaeoclimatol. Palaeoecol. 202, 1–29.
Caron M. 1985: Cretaceous planktic foraminifera. In: Bolli H. M.,
Saunders J. B. & PerchNielsen K. (Eds.): Plankton stratigraphy.
Cambridge Univ. Press, Cambridge, 17–86.
Caron M. & Homewood P. 1983: Evolution of early planktic
foraminifers. Mar. Micropaleontol. 7, 453–462.
Chacón B., Martínchivelet J. & Gräfe K.U. 2004: Latest Santonian to
Latest Maastrichtian planktonic foraminifera and biostratigraphy
of the hemipelagic succession of the Prebetic Zone (Murica and
Alicante provinces, southeast Spain). Cretaceous Res. 25,
585–601.
Čanović M. & Kemenci R. 1988: The Mesozoik of the Pannonian
basin in Vojvodina (Yugoslavia) — Stratigraphy and facies,
magmatism, paleogeography. Matica srpska, Novi Sad, 1–337
(in Serbian with English summary).
Čanović M. & Kemenci R. 1999: Geologic setting of the PreTertiary
basement in Vojvodina (Yugoslavia). Part II: The north part of
the Vardar zone in the south of Vojvodina. Acta Geol. Hung. 42,
4, 427–449.
Dulić. I., Sladić-Trifunović M., Žumberković V., Dunčić M. &
Bogićević G. 2004: Upper Cretaceous red beds of Serbia. 32
nd
International Geological Congress, Abstracts, Florence, 1, 2.
Dunčić M. & Bogićević G. 2008: Late Cretaceous microfossils of
Vojvodina, northern Serbia. 33
nd
International Geological
Congress, Abstract, Oslo, 198.
Fleury J.J. 1980: Les Zones de GavrovoTripolitza et du Pinde
Olonos (Grèce continentale et Péloponnèse du Nord). Evolution
d’une plateforme et d’un bassin dans leur cadre alpin. Ann. Soc.
Geol. Nord. 4, 2, 1–648.
Gajić V. 2014: Sedimentology Upper Cretaceous Central part of
Vardar Zone. Unpubl. Ph.D. Thesis, Univ. Belgrade, 1–260
(in Serbian with English abstract).
146
DUNČIĆ, DULIĆ, POPOV, BOGIĆEVIĆ and VRANJKOVIĆ
GEOLOGICA CARPATHICA
, 2017, 68, 2, 130 – 146
Gasiński M.A., Jugowiec M. & Ślączka A. 1999: Late Cretaceous
foraminiferids and calcareous nannoplankton from the
Weglówka Marls (Subsilesian Unit, Outer Carpathians, Poland).
Geol. Carpath. 50, 1, 6373.
Gušić I. & Jelaska V. 1990: Upper Cretaceous stratigraphy of the
island Brač within the geodynamic evolution of the Adriatic
carbonate platform. JAZU, Institut za geološka istraživanja,
Zagreb, 1–160.
Haas J., Hámor G., Jámbor Á., Kovács S., Nagymarosy A. &
Szederkényi T. 2012: Geology of Hungary. Regional Geology
Reviews, Budapest, 1–244.
Hradecká L., Lobitzer H., Ottner F., Švábenická L. & Svobodová M.,
1999: Biostratigraphy and Facies of selected Exposures in the
GrünbachNeue Welt GosauGroup (CoalBearing Series,
InoceramusMarl and ZweiersdorfFormation, Late Cretaceous
and Paleocene, Lower Austria). Abh. Geol. B.-A. 56, 2,
519–551.
Karamata S., Krstić B., Dimitrijević D.M., Dimitrijević M.N.,
Knežević V., Stojanov R. & Filipović I. 1997: Terranes between
the Moesian plate and the Adriatic sea. In: Papanikolaou D.
(Ed.): Annales géologiques des pays Helléniques, IGCP Project,
276. Terrane maps and terranes pescriptions 157,
Panepistimiopolis, Athines, 429–477.
Karamata S., Olujić J., Protić Lj., Milovanović D., Vujnović L.,
Popević A., Memović E., Radovanović Z & Resimić-Šarić K.
2000: The Western belt of the Vardar zone — the remnant of
a marginal sea. In: Karamata S. & Janković S. (Eds.): Proc.
Intern. Symp. Geol. and Metall. of Dinarides and the Vardar
Zone. Acad. Sci. and Arts of Rep. of Srpska, I, Depart. Nat.
Math. Techn. Sci., Banja Luka/Srpsko, Sarajevo, 131–135.
Karamata S., Sladić-Trifunović M., Cvetković V., Milovanović D.,
Šarić K., Olujić J. & Vujnović L. 2005: The western belt of the
Vardar Zone with special emphasis to the ophiolites of
Podkozarje — the youngest ophiolitic rocks of the Balkan
Peninsula. Bull. Acad. Serbe Sci. Arts, Classe Sci. Math. Nat.
CXXX, 43, 85–96.
Kędzierski M., Gasiński M.A. & Uchman A. 2015: Last occurrence
of Abathomphalus mayaroensis (Bolli) foraminiferid index of
the CretaceousPaleogene boundary: the calcareous nannofossil
proof. Geol. Carpath. 66, 3, 181–195.
Kemenci R. & Čanović M. 1987: Flysches of Vojvodina, The Torda
Flysch. In: Dimitrijević M. & M. (Eds.): The Turbidite Basins of
Serbia. Monographs, DLXXVI, Depart. Nat. Math. Sci. 61,
160–164.
Kemenci R. & Čanović M. 1997: Geologic setting of the PreTertiary
basement in Vojvodina (Yugoslavia). Part I: The Tisza Mega
unit of North Vojvodina. Acta Geol. Hung. 40, 1, 1–36.
Kuhnt W. 1990: Agglutinated foraminifera of western Mediterranean
Upper Cretaceous pelagic limestones (Umbrian Apennines, Italy
and Betic Cordillera, Southern Spain). Micropaleontology 36, 4,
297–330.
Kuhnt W. & Kaminski M.A. 1997: Cenomanian to lower Eocene
deepwater agglutinated Foraminifera from the Zumaya section,
northern Spain. Ann. Soc. Geol. Polon. 67, 257–270.
Loeblich A.R. & Tappan H. 1988: Foraminiferal genera and their
classification, Treatise on invertebrate paleontology. Univ.
of California, L.A, 1, 2, Van Nostrand Reinhold, New York,
1–970.
Machaniec E. & ZapalowiczBilan B. 2005: Foraminiferal
biostratigraphy and palaeobathymetry of Senonian marls (Upper
Cretaceous) in the vicinity of Kraków (JanuszowiceKorzkiew
area, Bonarka quarry) — preliminary study. In: Tyszka J.,
OliwkiewiczMiklasińka M., Gedl P. & Kaminski M.A. (Eds.):
Methods and Applications in Micropalaeontology. Stud. Geol.
Polon. 124, 285–295.
Murray J.W. 1991: Ecology and Palaeoecology of Benthic
Foraminifera. Longman Scientific & Technical, John Wiley and
Sons Inc., Essex, New York, 1–329.
Neumann M. 1997: Le genre Siderolites (Foraminifères). Révision
des différentes espèces, I
re
partie: Analyse bibliographique,
méthodologie, description des espèces du Campanien. Revue de
Micropaléontologie 40, 3, 227–271.
Ogg J.G. & Hinnov L.A. 2012: Chapter 28: Cretaceous. In: Gradstein
F.M., Ogg J.G., Schmitz M. & Ogg G. (Eds.): The Geologic Time
Scale 2012. Elsevier, Oxford, Amsterdam, Waltham, 793–853.
Olsson R.K. & Nyong E.E. 1984: A paleoslope model for Campanian
lower Maastrichtian foraminifera of New Jersey and Delaware.
Journal of Foraminiferal Research 15, 50–69.
Pamić J. 2002: The SavaVardar Zone of the Dinarides and Hellenides
versus the Vardar Ocean. Eclogae Geol. Helv. 95, 99–113.
Pamić J. & Šparica M. 1983: The age of the volcanic rocks of Požeška
Gora (Croatia, Yugoslavia). JAZU, Razred za prirodne znanosti
404, 19, Zagreb, 183–198 (in Croatian with English abstract).
Petrizzo M.R. 2002: Palaeoceanographic and palaeoclimatic
inferences from Late Cretaceous planktonic foraminiferal
assemblages from the Exmouth Plateau (ODP Sites 762 and 763,
eastern Indian Ocean). Mar. Micropaleontol. 45, 117–150.
Petrizzo M.R., Falzoni F. & PremoliSilva I. 2011: Identification of
the base of the lower to Middle Campanian Globotruncana
ventricosa Zone: comments on reliability and global correlations.
Cretaceous Res. 32, 387–405.
Premoli Silva I. & Sliter W.V. 1995: Cretaceous planktonic
foraminiferal biostratigraphy and evolutionary trends from the
Bottaccione section, Gubbio, Italy. Palaeontographia Italica 82,
I, 1–89.
Premoli Silva I. & Verga D. 2004: Practical manual of Cretaceous
planktonic foraminifera. In: Verga D. & Rettori R. (Eds.): 3
°
course Cretaceous planktonic Foraminifera. Universities of
Perugia and Milan, Tipografia Pontefelcino, Perugia, 1–283.
Robaszynski F. & Caron M. 1995: Foraminifères planctoniques du
Crétacé: commentaire de la zonation EuropeMéditerranée. Bull.
Soc. Géol. France 166, 6, 681–692.
Robaszynski F., Caron M., Gonzales Donoso J.M. & Wonders A.H.
1984: Atlas of Late Cretaceous Globotruncanids. Revue de
Micropaléontologie 26, 3–4, 145–305.
Robertson A., Karamata S. & Šarić K. 2009: Overview of ophiolites
and related units in the Late Palaeozoic–Early Cenozoic
magmatic and tectonic development of Tethys in the northern
part of the Balkan region. Lithos 108, 1–36.
Schmid M.S., Bernoulli D., Fügenschuh B., Matenco L., Schefer S.,
Schuster R., Tischler M. & Ustaszewski K. 2008: The Alps
CarpathiansDinaridesconnection: a correlation of tectonic
units. Swiss J. Geosci. 101, 139–183.
Schönfeld J. 1990: Zur Stratigraphie und Ökologie bentischer
Foraminiferen im SchreibkreideRichtprofil von Lägerdorf/
Holstein. Geol. Jahrb. A117, 1–151.
SladićTrifunović M. 1992: On the significance of Late Senonian rudist
faunas in Yugoslavia for reconstructions of the palaeobiogeographic
relations in Central Tethys. Comptes rendud des séances de la
Société Serbe de Géologie, livre jubilaire (1891–1991), 159–173
(in Serbian with English summary).
Ustaszewski K., Kounov A., Schmid S.M., Schaltegger U., Krenn E.,
Frank W. & Fügenschuh B. 2010: Evolution of the AdriaEurope
plate boundary in the northern Dinarides: From continent
continent collision to backarc extension. Tectonics 29, 6, TC6017.
van den Akker T.J.H.A., Kaminski M.A. & Gradstein F.M. 2002:
Campanian and Maastrichtian biostratigraphy in the Foula Sub
Basin, west of the Shetland Islands (UK). In: Wagreich M. (Ed.):
Aspects of Cretaceous Stratigraphy and Palaeobiogeography.
Österr. Akad. Wiss., öriftenr. Erdwiss. Komm. 15, 401–420.