www.geologicacarpathica.sk
GEOLOGICA CARPATHICA, JUNE 2009, 60, 3, 251—262 doi: 10.2478/v10096-009-0017-0
Introduction
The present study shows the results of ostracod analyses
from the Sadovi section (Mt Požeška gora, Croatia).
During the Early Miocene this area was located in the cen-
tral part of the North Croatian Basin, at the south-western
margin of the Pannonian Basin System (Fig. 1, Fig. 1.1). The
formation of the North Croatian Basin (in further text NCB)
was connected with passive continental rifting. A syn-rift
phase began during the Ottnangian and lasted until the Mid-
dle Badenian. The post-rift phase lasted from the Middle
Badenian to the Pliocene (Pavelić 2001).
In the NCB brackish ostracod assemblages are common in
Upper Miocene deposits (Sokač 1961, 1961a, 1963, 1965,
1967, 1972), but the presence of brackish ostracod faunas in
Lower Miocene deposits (Upper Ottnangian/Lower Karpa-
tian) at Sadovi locality is a new discovery.
The appearance of such fauna indicates the first ingression
of marine water into the Late Ottnangian/Early Karpatian
lake. In the uppermost part of the section Karpatian marine
marls concordantly overlay these brackish marls.
Geological setting
The Lower Miocene (Upper Ottnangian/Lower Karpatian)
deposits of the investigated section belong geotectonically to
the Pannonian Basin System and paleogeographically to the
south-western margins of the Central Paratethys. Central
Paratethys extends from Bavaria to the Carpathian mountain
chain (Steininger & Rögl 1979, 1984; Rögl & Steininger
1983, 1984; Rögl 1998, 1999). It was a part of the interconti-
nental bioprovince which began to evolve in the Oligocene
and was formed due to collision of the European (Tisa-Moe-
sia) and the African Plates (Horváth & Royden 1981; Kováč
et al. 1998).
Early Miocene ostracods from the Sadovi section
(Mt Požeška gora, Croatia)
VALENTINA HAJEK-TADESSE
1*
, MIRKO BELAK
1
, JASENKA SREMAC
2
, DAVOR VRSALJKO
1
and LARA WACHA
1
1
Croatian Geological Survey, Sachsova 2, 10 000 Zagreb, Croatia;
*
valentina.tadesse@hgi-cgs.hr
2
Faculty of Science, Department of Geology, Institute of Geology and Paleontology, Horvatovac 102 a, 10 000 Zagreb, Croatia
(Manuscript received November 8, 2007; accepted in revised form October 23, 2008)
Abstract: The study of the Early Miocene (Late Ottnangian/Early Karpatian) ostracod fauna from the Sadovi section
(Mt Požeška gora, Croatia) led to several results concerning Neogene paleobiogeography and paleoecology. Brackish
deposits of Late Ottnangian and Early Karpatian age have been recognized for the first time in the North Croatian Basin.
These deposits indicate the first marine ingression into the Early Miocene lake in this area. Twenty-nine ostracod species
were determined, including the new taxa Fabaeformiscandona slavonica nov. sp. and Herpetocypris sadovii nov. sp.
Key words: Late Ottnangian, Early Karpatian, North Croatian Basin, paleoecology, brackish environment, Ostracoda.
During the Miocene, connections of the Central Paratethys
with the Mediterranean and the Indo-Pacific Ocean were es-
tablished and interrupted several times (Steininger et al.
1988; Rögl 1996). Such unstable type of connection resulted
in sea-level oscillations (Haq 1991), different depositional
modes and paleoecological conditions, forcing the develop-
ment of different ostracod faunas.
In the Central Paratethys the Lower Miocene Ottnangian
stage (~ 18—17 Ma) is a twofold stage (Rögl et al. 1973). Ma-
rine conditions were dominant in the early phase of the Ott-
nangian. Except for the Northern Alpine Foreland Basin, no
entirely marine environments are known (Harzhauser & Piller
2005, 2007). During the Late Ottnangian, the Paratethys was
isolated from the Mediterranean Sea. This sea-level drop
seems to be linked with the global sea-level change of the
TB2.1 cycle, lasting from ~ 21—17.5 Ma (Haq 1991). Brack-
ish to freshwater sedimentary conditions prevailed, resulting
in the deposition of Rzehakia/Oncophora Beds in large areas
of the Paratethys (Rzehak 1882; Rögl & Steininger 1983;
Rögl 1998).
At the beginning of the late Early Miocene, during the glo-
bal sea-level cycle TB 2.2, lasting from ~ 17.5—16.4 Ma
(Haq 1991), the sea-level rose and the Karpatian stage
(~ 17—16.3 Ma) began with transgressions. In different ba-
sins, Karpatian deposits were discordantly deposited over
the Ottnangian marine shales, in littoral settings over the
Rzehakia Beds, continental deposits or over older basement
units (Rögl et al. 2003). A continuous transition between the
Ottnangian and the Karpatian is expected only in deeper
parts of the Central Paratethys, whereas all shallow marine
settings display a strong discordance (Rögl et al. 2003).
In the NCB the Lower Miocene lowstand deposition is
represented mainly by alluvial, fluvial and deltaic deposits.
At the base of the Karpatian, this sequence is rapidly re-
placed by marine neritic to shallow bathyal sediments
(Pavelić 2001).
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HAJEK-TADESSE, BELAK, SREMAC, VRSALJKO and WACHA
Formation of a sedimentary basin in the area of the
Slavonian Mts started in the Ottnangian with freshwater de-
posits (Pavelić et al. 1998). Two depositional phases were
recognized by Pavelić (2001). The first phase was character-
ized by the accumulation of predominantly breccias and con-
glomerates with subordinate sand and siltstones deposited in
a braided alluvial plain and under semi-arid climate condi-
tions (Pavelić et al. 1998). During the second depositional
phase a freshwater lake was formed in the area of the
Slavonian Mts, in which silts and sands with sporadic layers
of gravels, tuffs and tuffites were deposited. The endemic os-
tracod and molluscs faunas are found together with fossil
plants (Pavelić et al. 1998). The second depositional phase
was characterized by a shift to humid climate conditions.
Lacustrine conditions were replaced by marine environments
during the Karpatian time (Pavelić 2001).
Study site and methods
Study site
The Sadovi section is located in
the southern part of Mt Požeška
gora on the top of the Sadovi
hills, along a forest road. The sec-
tion is about 500 m long, and the
total real thickness of the Lower
Miocene sequence is 150 m. All
32 samples were collected from
marls (Fig. 2). Besides the ostra-
cods, remains of plants, molluscs
and fishes were found. The colour
of the marls varies from yellow,
brownish-grey to olive-green.
In the first 30 meters of the sec-
tion, the marls are laminated and
rich in plant fragments, ostracods
and fish bones. In the central part
of the section (65—80 m) the marls
are laminated, contain thin films of
bitumen and rich ostracod faunas.
Twenty five meters of the section
are not exposed. Between samples
Sa 29 and Sa 30, the contact with
the Karpatian marine sediments
has been noticed.
Methods
The collected marl samples were
disaggregated by soaking in a hy-
drogen peroxide solution for 24
hours, then washed through sieves
(0.5; 0.25; 0.125; 0.063 mm) and
dried. Some of the samples needed
extra cleaning and were soaked
again in hydrogen peroxide and
treated ultrasonically for approxi-
mately 20 seconds. 100 g of each
dried residue was observed under a
Fig. 1. Geographic setting of the North Croatian Basin within the Pannonian Basin System (after
Pavelić 2001). Fig. 1.1. Location map of Mt Požeška gora
with marked position (•) of the Sa-
dovi section (after Pavelić 2001).
stereomicroscope. Ostracods and other remains (foraminifers
and gastropods) were hand-picked, counted and determined.
Ostracods were picked qualitatively but not selectively, in or-
der to preserve the relative composition of the thanatocoenose.
Six samples were selected for insoluble residue and car-
bonate content analysis. They were treated with 10% HCl
and the carbonate content was measured. The insoluble resi-
due, after treatment with HCl, was washed and thin sections
were prepared.
Photographs were made with a SEM at the Geological De-
partment of the Faculty of Science in Zagreb. For photo-
graphing we used two different detector types: BSE – Back
Scatter Detector and SE – Secondary Electron Detector.
All ostracod specimens are stored in the archive collection
of the Croatian Geological Survey (Inv. No. HGI-CGS Hr/Sa
2006/HTV).
253
EARLY MIOCENE OSTRACODS FROM THE SADOVI SECTION (CROATIA)
Results
Ostracod distribution
Altogether, 29 species belonging to 18 genera and 5 fami-
lies (Darwinulidae, Candonidae, Cyprididae, Limno-
cytheridae and Cytherideidae) were identified. Some of the
taxa (13) remain in open nomenclature, 6 species are left in
open nomenclature, two species are new (Table 1).
Fig. 2. Stratigraphical log of the Sadovi section.
A brackish ostracod fauna was found in 26 samples. Only
the uppermost three samples (Sa 30—32) of the section repre-
sent a marine fauna; we recognized juvenile valves of marine
Karpatian ostracods (Henryhowella sp.), and benthic and
planktonic foraminifers (Svratkina sp., Coryphostoma cf.
digitalis, Tenuitella sp., Globigerinoides sp., Cassigerinella
globulosa). This environmental change was caused by the
influx of sea water into the lake. The marine depositions will
not be part of this investigation. Three samples (Sa 4, Sa 5,
Sa 14) did not yield any fossils.
The most abundant and frequent species in the samples
from the Sadovi section are: Herpetocypris sp. (22 records),
Candona (Pontoniella) sp. and Candona sp. (both 13 records)
and Fabaeformiscandona pokornyi (11 records). The diversity
varies throughout the section, and is generally low.
The maximum number of species (11) was reported in
samples Sa 2 and Sa 9. Other samples with relatively high
numbers of species are Sa 18 (10 species), Sa 7 (9 species)
and Sa 1, Sa 10, Sa 28 (8 species). In other samples the num-
ber of species varies between 4 and 8, and 5 samples contain
only 2 species.
The identified ostracod species (Table 1) can be divided
into two groups. The first group includes the species from
samples 1 to 18 of Sadovi section. These samples point to a
brackish environment with salinities ranging from oligoha-
line or (low) mesohaline.
The second group is represented by the species from sam-
ples 19 to 29, which indicate the gradual decrease of salinity.
A few species appear exclusively in the first group: Fa-
baeformiscandona slavonica nov. sp., Cyprideis sublittora-
lis, Heterocypris cf. francofurti, Amplocypris sp., Cypris sp.,
Darwinula stevensoni, Eucypris cf. dulcifons, Paralimno-
cythere rostrata, and three Potamocypris species: P. fulva,
P. cf. gracilis, P. cf. arcuata. The accompanying species are
Fabaeformiscandona pokornyi, Candona (Caspiolla) sp.,
Candona (Pontoniella) sp., Cypridopsis biplanata, Herpeto-
cypris sp. and Herpetocypris sadovii nov. sp. In the upper-
most part of the first level Candona (Lineocypris) sp. and
Candona (Typhlocypris) sp., have the first common occur-
rence. A single valve of Aurila sp. and a few benthic fora-
minifers Aubignyna perlucida were found in sample Sa 2.
The second group of samples (from Sa 19 to Sa 29) con-
tains most of the species from the first group. The dominant
species in the second group are Herpetocypris sp., Fabaefor-
miscandona pokornyi and Candona (Pontoniella) sp.
Herpetocypris sp. gradually becomes more common from the
end of the first level to the end of the section. The species which
are present only in the second group with very few valves are
Pseudocandona praecox, Mediocypris cf. candonaeformis and
Dolerocypris sp. In contrast to the first group Candona
(Typhlocypris) sp. is more common in the second group.
Candona (Lineocypris) sp., Candona (Caspiolla) sp., Cypria
sp. and Herpetocypris sadovii nov. sp. occur only in the upper-
most samples of the second group. Cypria dorsalta, Cypri-
dopsis biplanata and Eucypris sp. are present with few valves.
The brackish ostracod fauna is autochthonous, and well
preserved. The population structure of the ostracod fauna in-
dicates low water energy of the environments and low sedi-
mentation rates (Whatley 1983).
254
HAJEK-TADESSE, BELAK, SREMAC, VRSALJKO and WACHA
Mineralogical analyses and carbonate content
Carbonate content in marl samples SA 4, SA 7, SA 14,
SA 16 and SA 19 varies from 46.3 to 55.0 %. Sample SA 30
is a clay rich marl with 13.1% carbonate content. Samples
from Sadovi contain a very small amount of silty siliciclastic
detritus. The mineral composition of the insoluble residue in
the analysed samples is quite homogeneous. Non-undulose
monocrystalline subrounded or subangular quartz grains and
altered feldspar grains dominate. Non-altered feldspars and
twinned plagioclase are less abundant. The lithic fragments
are scarce, with domination of shale fragments and some
chert fragments.
A very small amount of heavy minerals is present in the
samples. The most abundant among them are resistent tur-
maline and garnet, accompanied by rutile, zircon, staurolite,
amphibole, titanite, biotite and chlorite. Opaque minerals are
also present. In the sample SA 19 opaque minerals dominate,
while the composition of the translucent heavy minerals is
the same as in other samples.
The source of clasts could be related to igneous and meta-
morphic rocks from the vicinity. The small amount of silici-
clastic components indicates calm depositional conditions
and a very restricted terrigenous input.
Discussion
Ostracods from brackish waters are valuable tools in paleo-
environmental reconstruction and in environmental studies.
The main parameters which can be monitored with brackish
water ostracods are salinity and hydrochemistry, water
depth, substrate, oxygen and productivity, temperature and
climate (Frenzel & Boomer 2005). The composition of ostra-
cod assemblages from our section depends mainly on the sa-
linity and depth of the lake water.
Table 1: Distribution of the Ostracoda in the Lower Miocene deposits of the Sadovi section (1—18 = transgressive phase; 19—29 = regres-
sive phase). Only adult valves for each species in the samples were counted:
1—2,
2—5,
5—10,
10—20,
20—40.
255
EARLY MIOCENE OSTRACODS FROM THE SADOVI SECTION (CROATIA)
Brackish-water ostracods are normally found in transitional
environments or in inland saline lakes (Remane 1971). The
different biotopes appear and disappear at various levels in a
stratigraphic succession, following the dynamics of transgres-
sion and regression through time (Do Carmo et al. 1999). In
the Western Paratethys, the Late Ottnangian regression initiat-
ed the development of a shallow brackish basin, and presence
of planktonic larval development in gastropods indicates a
connection with the open sea (Kowalke & Reichenbacher
2005). In the Sadovi section deposition of Upper Ottnangian
and Lower Karpatian brackish water sediments is a conse-
quence of a marine ingression into the freshwater lake, which
is the first signal of the new transgression in the Karpatian.
During the Early Ottnangian a freshwater lake existed in the
area of the Mt Požeška gora (Kochansky-Devidé 1979;
Pavelić et al. 1998; Pavelić 2001). The oldest alluvial and lake
clayey deposits lack ostracods, and marly sediments of a olig-
otrophic freshwater lake contain ostracod communities
(Hajek-Tadesse et al. 2006).
The increase of water salinity in the Late Ottnangian and
Early Karpatian, which is observed in the Sadovi section for
the first time, was caused by the ingression of marine water
into the lake. Ingression of marine water was documented by
the composition of ostracod fauna, especially with the occur-
rence of typical brackish ostracod taxa: Cyprideis sublittora-
lis and Aurila sp. together with scarce foraminifers
(Aubignyna perlucida).
The occurrence of the genus Cyprideis in the Sadovi sec-
tion plays an important role in the identification of brackish
environments. The genus Cyprideis is not typical for the
Lower Miocene deposits of the Central Paratethys. It is com-
mon in the Upper Miocene deposits of Croatia (Sokač 1972).
For the Late Sarmatian and Pannonian (12 to 8.5 Ma) in the
Molasse Basin, the occurrence of Cyprideis spp. and can-
donid species indicate brackish conditions (Janz & Venne-
mann 2005).
In Europe the probable ancestor of the genus Cyprideis is
Miocyprideis (Kollmann 1960). The evolutionary sequence of
Cyprideis in the Amazon Basin began in the Early Miocene,
and the most explosive radiation of Cyprideis in Western
Amazon region occurred at the boundary between the Early
and Middle Miocene (Langhian stage). The ancestors of Cyp-
rideis in the Amazon Basin are not identified. A paleofauna of
21 endemic species of the euhaline genus Cyprideis lived be-
tween polyhaline and oligohaline salinity ranges during spo-
radic intervals of marine influence (Mu oz-Torres et al. 2006).
In contrast to brackish Rzehakia/Oncophora Beds of the
Central Paratethys, which is a result of global sea-level de-
crease, Lower Miocene brackish deposits in Sadovi are the re-
sult of marine ingression.
Numerous paleosalinity studies were based on the cosmopol-
itan holoeuryhaline species Cyprideis torosa. Aladin (1993)
pointed out that C. torosa is a brackish water ostracod of marine
origin with extremely complex osmoregulatory mechanisms
and is known to withstand low oxygen conditions.
Lateral sieve pores of recent and fossil Cyprideis torosa
vary in outline from round to oval and irregular. The percent-
age of round pores decreases with the increase of salinity
(Rosenfeld & Vesper 1977).
Gliozzi & Mazzini (1998) and Anadon et al. (2002) note
that differences in paleosalinity values may be explained by
mixing waters of different origin.
A connection between the salinity and noding of C. torosa
was noticed by Hartmann (1964), Vesper (1975), Van Harten
(1996) and Keyser (2005). Noding at low salinities is the most
accepted condition, despite the fact that the controlling mech-
anism is poorly understood. Do Carmo et al. (1999) connect
variable noding of Middle Jurassic limnocytherid ostracods
with salinity changes.
In the first group (transgressive part) of the Sadovi samples,
rounded, oblong and irregularly shaped sieve pores of the spe-
cies Cyprideis sublittoralis are distributed in almost even per-
centage. Rosenfeld & Vesper (1977) connected such
distribution with 8 to 16 ‰ salt concentration. On the other
hand, in these samples we found only unnoded forms of adults
and numerous juvenile stages. Brackish water ostracods live
within the uppermost few millimeters of the sediment, be-
cause much of the sediment below this level is often rich in or-
ganic material and, as a result, depleted in oxygen (Horne &
Boomer 2000).
The ostracod fauna from Sadovi can be compared with the
brackish ostracods from the Kirchberg Formation (Upper
Ottnangian/Lower Karpatian) of the western part of the
South German Molasse Basin (Witt 2000) and ostracods
from the Oncophora Beds in the East (Witt 1999), but ostra-
cod assemblages from Sadovi are indicative for a more sa-
line lake environment.
Such faunal relations are more common in the Late Mi-
ocene of the Paratethys area: Styrian Basin, Turčianska kotli-
na Depression (Slovakia) and the Pannonian Basin (Sokač
1972; Gross 2004; Pipík & Bodergat 2004).
Beside salinity, substrate is the main factor controlling the
occurrence of ostracods in brackish water (Ruiz et al. 2000).
The marl deposits in the Sadovi section are horizontally lami-
nated, they contain thin bituminous lamina, rich ostracod as-
semblages, plant remains and a few skeletal fish particles.
During the Late Ottnangian and Early Karpatian in the area
of Mt Požeška gora an eutrophic lake existed with increasing
salinity of water and low input of clastic material from the
land. We recognized this event as the new, “third phase” of
deposition in NCB sensu Pavelić (2001).
Most of the ostracod taxa determined from the Sadovi sec-
tion prefer ponds and lakes and tolerate an increase of salinity
(Meisch 2000). Dissolution of valve margins in the species
Amplocypris sp. and bacterial activities on Cypria dorsalta
valves are a common effect and are typical for eutrophic envi-
ronments (Reeves et al. 2007).
Carbonel et al. (1988) conclude that species with “high” tri-
angular, trapezoidal shape and elongated valves with pointed
posterior (such as Candona (Lineocypris) sp., Candona
(Typhlocypris) sp., Candona (Pontoniella) sp. and Cypris sp.
from Sadovi) occur frequently in persistent environments with
low environmental fluctuations like groundwater habitats and
the sublittoral of old lakes.
The confirmation of marine ingression into the Late Ott-
nangian/Early Karpatian lake in the area of Mt Požeška
gora gives a key for understanding the formation of analci-
me deposits north and south-east from the investigated sec-
ñ
256
HAJEK-TADESSE, BELAK, SREMAC, VRSALJKO and WACHA
tion. Ščavničar et al. (1983) studied the analcime-bearing
deposits north of Sadovi in Poljanska (southern Papuk,
Slavonija region) and Sirječić et al. (1974) described analci-
molites south-east from Sadovi, in the Tuzla salt series (Bos-
nia and Herzegovina).
The genesis of sediments near Poljanska is linked to the
saline alkaline lake environment. Ščavničar et al. (1983)
conclude that analcime was formed by alternation of volca-
nic glass, as well as from other silicates in the shallow water
of an unsheltered saline alkaline lake, under conditions of in-
creasing aridity and closure of the lake. Variable composi-
tion, texture and structure of analcime-bearing deposits give
the evidence of the climate shifts and the lake history
(Ščavničar et al. 1983).
The registered influx of marine water into the lake before
the Karpatian transgression and the appearance of the brack-
ish ostracod fauna at Sadovi raise new questions on marine
connections between the Mediterranean and the Central
Paratethys.
The problem of the marine connection between the Medi-
terranean and Central Paratethys area remains unsolved. The
Transtethyan Trench Corridor (Bistričić & Jenko 1985) was
situated somewhere in the territory now forming part of Slo-
venia or northern Croatia. On the basis of our previous in-
vestigations and the results of our work in this paper we
conclude that the possible position of the new corridor,
which has not previously been well documented, is south-
east of the NCB.
Conclusions
The study of ostracod assemblages from Sadovi revealed
for the first time the existence of brackish deposits in the
Late Ottnangian/Early Karpatian, as a result of marine in-
gression into the lacustrine water of the NCB. In the upper-
most samples of the investigated section a continuous
transition of brackish deposits into the Karpatian marine
beds with scarce marine microfauna was observed.
The microfauna from the Sadovi section belong to the up-
per part of the Lower Miocene (Upper Ottnangian/Lower
Karpatian). A more precise biostratigraphic dating is not
possible on the basis of ostracods. However, paleoecological
data obtained by ostracod analysis are much more signifi-
cant. For the first time, based on ostracod assemblages, a
wide brackish influence could be documented in the Lower
Miocene deposits of the NCB.
Samples from the Sadovi section can be divided into two
groups. The groups are defined on the basis of different os-
tracod assemblages and different trends in water salinity. In
the first group (samples 1—15) we found brackish ostracod
assemblages with the indicative brackish species Cyprideis
sublittoralis, which has been detected for the first time in the
Lower Miocene of the Central Paratethys. In the second
group (samples 16—25) these species disappear and ostracod
assemblages indicate the slight decrease of water salinity.
Qualitative analyses resulted with 29 identified ostracod
species, among which two species are new: Fabaeformiscan-
dona slavonica nov. sp. and Herpetocypris sadovii nov. sp.
Brackish deposits of the Sadovi section are the result of
the marine ingression into the lake. They represent the “third
phase” of development, of the NBC successively comple-
menting the local reconstruction of the Ottnangian deposi-
tional model introduced by Pavelić (2001).
The genesis of analcime layers north and south-east of the
investigated area (Sirječić et al. 1974; Ščavničar et al. 1983)
can also be explained by the intrusion of sea water into the
Early Miocene lake.
The detected brackish Lower Miocene (Upper Ottnangian/
Lower Karpatian) deposits of the “third phase” and transgres-
sive Karpatian marine marls, indicate the possibility of an addi-
tional marine connection between the Mediterranean and/or
Indo-Pacific Ocean situated south-east of the investigated area.
Acknowledgments: The authors wish to thank Professor
Ana Sokač for her comments and discussion about the ostra-
cod fauna. Professor Vladimir Bermanec and Hrvoje Posi-
lović, B.Sc. from the Faculty of Science, Zagreb provided us
with SEM microphotographs. The authors are very grateful
to Ivo Suša from the Croatian Geological Survey for techni-
cal support.
Appendix
New ostracod species
The following abbreviations are used in the description of
the new ostracod species: LV and RV – left and right
valves; H and L – height and length; n – number of mea-
sured specimens; and – female and male.
Class: Ostracoda Latreille, 1806
Order: Podocopida Sars, 1866
Suborder: Podocopina Sars, 1866
Superfamily: Cypridoidea Baird, 1845
Family: Candonidae Kaufmann, 1900
Subfamily: Candoninae Kaufmann, 1900
Genus: Fabaeformiscandona Krstić, 1972
Generic characters of this new species are according to
those given by Van Morkhoven (1962). Carapace usually
elongated in lateral view, greatest H close to 1/2 L. Mostly
with significant sexual dimorphism. LV usually with poste-
ro-dorsal lobe, overlapping the RV (diagnosis after Meisch
2000).
The genus Fabaeformiscandona comprises ca. 50 recent
species (Meisch 2000). The oldest fossil representatives of
this genus are known from the Early and Middle Miocene of
Europe (Janz 1997; Witt 1998, 2000; Schäfer 2005). Some
recent species of the genus Fabaeformiscandona frequently
occur in Pliocene and Pleistocene (Meisch 2000).
Fabaeformiscandona slavonica nov. sp.
Fig. 3.1—7
M a t e r i a l : 46 valves.
♀
♂
257
EARLY MIOCENE OSTRACODS FROM THE SADOVI SECTION (CROATIA)
Fig. 3. SEM microphotographs of selected ostracods. 1 – Fabaeformiscandona slavonica nov. sp., Sa 2, male right valve, external view
(SE Detector). 2 – Fabaeformiscandona slavonica nov. sp., Sa 2, male left valve, external view (SE Detector). 3 – Fabaeformiscandona
slavonica nov. sp., Sa 2, female right valve, external view (SE Detector). 4 – Fabaeformiscandona slavonica nov. sp., Sa 3, female left
valve, external view (SE Detector). 5 – Fabaeformiscandona slavonica nov. sp., Sa 2, female right valve, external view (BSE Detector).
6 – Fabaeformiscandona slavonica nov. sp., Sa 2, female left valve, internal view (BSE Detector). 7 – Fabaeformiscandona slavonica
nov. sp., Sa 2, female carapace, seen from the right (SE Detector).
258
HAJEK-TADESSE, BELAK, SREMAC, VRSALJKO and WACHA
E t y m o l o g y : Type locality is situated in Slavonia, re-
gion in eastern Croatia.
H o l o t y p e : Right valve, Fs-1, HGI-CGS Hr/Sa 2006/
HTV. Fig. 3.1.
T y p e - l e v e l : Lower Miocene/Upper Ottnangian—Lower
Karpatian, brackish deposits.
T y p e - l o c a l i t y : Sadovi, Mt Požeška gora, North Croat-
ian Basin.
P a r a t y p e s :
Left valve Fs-2, HGI-CGS Hr/Sa 2006/HTV. Fig. 3.2.
Right valve Fs-3, HGI-CGS Hr/Sa 2006/HTV. Fig. 3.5.
Left valve Fs-4, HGI-CGS Hr/Sa 2006/HTV. Fig. 3.4.
D i a g n o s i s : Fabaeformiscandona slavonica is best rec-
ognized in the external lateral view of right valve. The dorsal
margin of RV is specific with swale.
D e s c r i p t i o n : Valves smooth, strongly calcified, with
variable H/L ratio; greatest H situated distinctly behind mid—
length. Carapace laterally compressed in dorsal view. Dorsal
margin of the LV overlaps the RV. Sexual dimorphism present.
Male. Valves elongated less high than in the female. Dor-
sal margin slightly convex. Ventral margin slightly concave.
Anterior end rounded. Posterior end almost straight and ob-
liquely cut, forming a sharp angle with the postero-ventral
margin. LV (interior) slightly turned inwards in the upper
part of the posterior end. Males always present.
Female. RV with similar shape to male RV, slightly higher
than male. RV with swale on dorsal margin. LV with distinct
convex dorsal margin, gently and continuously sloping
down towards anterior and posterior ends (swale missing).
While anterior end is gently rounded, posterior end is almost
evenly cut off, forming a small point with the afferent ven-
tral margin. LV with maximum width in the central part.
M e a s u r e m e n t s (mm):
Holotype RV (Fs-1, HGI-CGS Hr/Sa 2006/HTV):
L = 1.04, H = 0.43.
Paratype LV (Fs-2, HGI-CGS Hr/Sa 2006/HTV):
L = 1.02, H = 0.38.
RV (Fs-3, HGI-CGS Hr/Sa 2006/HTV): L = 1.01,
H = 0.53.
LV (Fs-4, HGI-CGS Hr/Sa 2006/HTV): L = 1.02,
H = 0.54.
R a n g e s o f s i z e s o f s e l e c t e d s p e c i m e n s :
L (LV) = 1.03—0.99 mm (n=2); H (LV) = 0.39—
0.36 mm (n = 2).
L (LV) = 0.98 mm (n=1); H (LV) = 0.49 mm (n = 1).
L (RV) = 1.03—0.94 mm (n = 5); H (RV) = 0.41—
0.37 mm (n = 5).
L (RV) = 1.00—0.96 mm (n = 2); H (RV) = 0.51—
0.49 mm (n = 2).
R e m a r k s : The Fabaeformiscandona slavonica nov. sp.
has to be compared to the known described Miocene species:
Fabaeformiscandona fabaeformis (Fischer) and F. cf. bala-
tonica (Daday) (sensu Janz 1997: p. 3, figs. 3—10; p. 4,
figs. 1, 2); F. pokornyi (Kheil) (sensu Witt 1998: p. 1,
figs. 2—8; 2000: p. 2, fig. 3); and Fabaeformiscandona sp.
(sensu Schäfer et al. 2005: p. 2, figs. 9—11), however, none is
close to the new species.
Other Fabaeformiscandona species have been investigated.
The new species differs from all of these. In general, Fabae-
formiscandona slavonica nov. sp. can easily be distin-
guished from all its congeners in the postero-dorsal part of
the male and female RV. Only the carapace of recent Fabae-
formiscandona fabaeformis (Fischer) is similar in dorsal
view. Female LVs of Fabaeformiscandona slavonica nov.
sp., resemble those of Fabaeformiscandona levanderi (Hir-
schmann) in shape. The female LVs can easily be distin-
guished from each other by the posterior and postero-ventral
part of the valve.
Family: Cyprididae Baird, 1845
Subfamily: Herpetocypridinae Kaufmann, 1900
Genus: Herpetocypris Brady & Norman, 1889
The new species belongs to the genus Herpetocypris. Car-
apace elongated in lateral view, about 1.5—2.6 mm long. The
height always less than half the length. Both ends are round-
ed. Dorsal margin weakly rounded to almost straight. Cara-
pace laterally moderately compressed. Fused valve zones
small, pore canals straight, marginal septae absent. LV over-
laps RV along the entire valve margin (diagnosis after Van
Morkhoven 1963; Meisch 2000).
Six certain and several dubious species have been record-
ed from Europe (Meisch 2000). Fossil species of Herpeto-
cypris are known from the Early and Middle Miocene of
Europe (Sokač 1979; Sokač & Krstić 1987; Jurišić-Polšak et
al. 1993; Witt 1999, 2002). The fossil records for some re-
cent species of genus Herpetocypris are common from the
Pleistocene (Van Morkhoven 1963; Meisch 2000).
Herpetocypris sadovii nov. sp.
Fig. 4.1—3
M a t e r i a l : 15 valves.
E t y m o l o g y : After the type section in which it was first
found.
H o l o t y p e : Right valve, Hb-1, HGI-CGS Hr/Sa 2006/
HTV. Fig. 4.3.
T y p e - l e v e l : Lower Miocene/Upper Ottnangian—Lower
Karpatian, brackish deposits.
T y p e - l o c a l i t y : Sadovi, Mt Požeška gora, North Croat-
ian Basin.
P a r a t y p e : Left valve Hb-2, HGI-CGS Hr/Sa 2006/
HTV, sample Sa 10.
D i a g n o s i s : Distinctly elongated valve with rounded an-
terior and posterior end.
D e s c r i p t i o n : A large, elongate, well calcified valve.
Smooth surface. Dorsal margin almost straight in the middle
and sub parallel to the ventral line. Transitions from dorsal
margin to anterior and posterior ends are gradual. Ventral mar-
gin slightly concave in the middle. Anterior and posterior end
rounded, but anterior end broader than the posterior one.
Fused valve zones small. Marginal pore canals strait and
short. Muscle scars weakly evident. No distinct sexual di-
morphism could be detected in the examined material.
M e a s u r e m e n t s (mm):
Holotype RV Hb-1, HGI-CGS Hr/Sa 2006/HTV:
L = 1.34, H = 0.48.
♂
♂
♀
♀
♂
♂
♂
♂
♀
♀
♀
♀
259
EARLY MIOCENE OSTRACODS FROM THE SADOVI SECTION (CROATIA)
Fig. 4. SEM microphotographs of selected microfossils. 1 – Herpetocypris sadovii nov. sp., Sa 9 right valve, external view (SE Detector).
2 – Herpetocypris sadovii nov. sp., Sa 10 right valve, internal view (SE Detector). 3 – Herpetocypris sadovii nov. sp., Sa10, right valve,
external view (SE Detector). 4 – Herpetocypris sp., Sa 19, right valve, external view (SE Detector). 5 – Cyprideis sublittoralis Pokorný,
Sa 2, female left valve, external view (SE Detector). 6 – Cyprideis sublittoralis Pokorný, Sa 2, male right valve, external view (BSE De-
tector). 7 – Cyprideis sublittoralis Pokorný, Sa 2, selected detail of left valve, with central muscle scars and sieve pores (BSE Detector).
8 – Aurila sp., Sa 2, left valve, external view (SE Detector). 9 – Aubignyna perlucida (Heron-Allen & Earland), Sa 2 (SE Detector).
260
HAJEK-TADESSE, BELAK, SREMAC, VRSALJKO and WACHA
Fig. 5. SEM microphotographs of selected ostracods. 1 – Candona (Typhlocypris) sp., Sa 22, left valve, external view (SE Detector). 2 – Cypris
sp., Sa 9, left valve, external view (SE Detector). 3 – Cypria dorsalta Malz & Moayedpour, Sa 7, left valve, external view (BSE Detector).
4 – Potamocypris cf. arcuata Sars, Sa 10, left valve, external view (SE Detector). 5—6 – Candona (Pontoniella) sp., Sa 24, right valves,
external view (SE Detector). 7 – Candonopsis sp., Sa 2, right valve, external view (SE Detector). 8 – Candona (Caspiolla) sp., Sa 12, right
valve, external view (SE Detector). 9 – Fabaeformiscandona pokornyi (Kheil), Sa 20, left valve, external view (SE Detector). 10 – Can-
dona sp., Sa 12, right valve, external view (SE Detector).
261
EARLY MIOCENE OSTRACODS FROM THE SADOVI SECTION (CROATIA)
Paratype LV Hb-2, HGI-CGS Hr/Sa 2006/HTV:
L = 1.19, H = 0.46.
L (LV) = 1.21 mm (n = 1): H (LV) = 0.46 mm (n = 1).
L (RV) = 1.33—1.29 mm (n = 3): H (RV) = 0.47—0.42 mm
(n = 3).
R e m a r k s : Herpetocypris sadovii nov. sp. comes close
to Herpetocypris chevreuxi (Sars). The two species differ in
the following characters: a) size – H. chevreuxi are longer
than H. sadovii; b) ventral margin – in Herpetocypris sa-
dovii nov. sp. ventral margin is more concave; c) posterior
end – different shape in postero-dorsal part of valve. The
new species Herpetocypris sadovii differs from the Early
and Middle Miocene Herpetocypris species: Herpetocypris
sp. A (sensu Witt 1999: p. 2, fig. 6—9; 2002: p. 2, fig. 5—8);
Herpetocypris snegotini (Krstić) (sensu Sokač 1979: p. 2,
figs. 1, 3, 5); Herpetocypris sp. (sensu Jurišić-Polšak et al.
1993: p. 1, figs. 1, 6, 9, 12) in shape of valves, especially in
area of dorsal margin, and anterior/posterior ends.
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