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Abstract
In the Styrian Basin, early Miocene marine sedimentation of the Karpatian (upper Burdigalian) ended with basin shallowing, mar-
rd
ked regression and tectonic movements. The Karpatian sedimentation cycle corresponds to the global 3 order cycle TB 2.2, follo-
wed by the Bur5/Lan1 sea-level fall. This regression was combined with tectonic movements (the Styrian Tectonic Phase), seen in
the Styrian Unconformity by an angular discordance at the Wagna and Katzengraben outcrops and also in deep wells. Sediments of
the first middle Miocene (Badenian/Langhian) transgression are commonly eroded or reduced in thickness at the basin borders. In
the basin center, the bathyal environment continues from the Karpatian to the Badenian. Sediments of the first Badenian transgres-
sion have been dated by calcareous nannoplankton as NN4 and correlated by the occurrence of Praeorbulina sicana with the basal
rd
Langhian. The 3 order sequence corresponds to TB 2.3. The erosional phase of the sea-level fall Lan2/Ser1 can only be observed
in near-shore facies, followed by transgressive beds within Zone NN5, which represents the second, main Badenian transgression
in the Central Paratethys and corresponds to the long global cycle TB 2. The highstand system tract of this cycle is expressed in
rd
carbonate build-ups of the Weissenegg Formation. According to the global 3 order sequences, the youngest sediments of the
Retznei section (< 14.39 Ma) overlying the carbonate buildups belong to the falling-stage system tract of TB2, but did not record
regression, but instead continuous deepening of the Styrian Basin, indicating strong subsidence during the early middle Miocene.
Die marine Sedimentation während des älteren Miozäns (Karpatium / Oberes Burdigalium) endete im Steirischen Becken mit einer
starken, durch tektonische Bewegungen verstärkten Regression. Der Sedimentationszyklus im Karpatium entspricht der globalen
Sequenz TB 2.2 und wird durch das Absinken des Meeresspiegels (Bur5/Lan1) begrenzt. Die Kombination der Regression mit den
tektonischen Bewegungen („Steirische Tektonische Phase“) ist als Winkeldiskordanz und Sedimentationsunterbrechung („Styrian
Unconformity“) sowohl in den Tagesaufschlüssen Wagna und Katzengraben, als auch in Tiefbohrungen ausgebildet. Sedimente der
folgenden, ersten Transgression im Badenium/Langhium sind in den Randbereichen des Beckens zumeist erodiert oder nur spärlich
erhalten, während im Beckeninneren durchwegs bathyale Sedimente sowohl im Karpatium als auch im Badenium auftreten. Die fol-
gende Transgression im Badenium läßt sich anhand des kalkigen Nannoplanktons in die Nn4 Zone stellen und korreliert wegen des
Auftretens der planktonischen Foraminifere Praeorbulina sicana mit dem basalen Langhium. Die Sequenz 3. Ordnung entspricht der
TB 2.3. Die erosive Phase an der Lan2/Ser1 Grenze ist in den Randbereichen des Beckens als Sedimentationsunterbrechung aus-
geprägt, die von der 2. Transgression im Badenium, der Haupttransgression innerhalb der Paratethys, gefolgt wird. Letztere ent-
spricht dem globalem Zyklus TB 2. Karbonate der Weissenegg-Formation kennzeichnen im Steirischen Becken den Höhepunkt die-
ser Trangression. Die über den Karbonaten folgenden Siliziklastika müssten entsprechend der Sequenzstratigraphie als zum „falling
stage system tract“ gehörend eine Regression anzeigen, sie kennzeichnen aber durch das kontinuierliche Absinken des Meeresbo-
dens die tektonisch bedingte Subsidenz des Steirischen Beckens im Laufe des älteren Mittleren Miozäns.
_
____________________
Austrian Journal of Earth Sciences Vienna
1. Introduction
During the early Miocene, the region of the circum-Mediter-
ranean, including the vast area of the Paratethys, underwent
profound changes. The Mediterranean was cut off from the
Indian Ocean; the Eastern Paratethys became an isolated
basin and the sea regressed from the Alpine Foredeep in the
West and from the Transylvanian Basin, reducing the Central
Paratethys marine realm to the Pannonian Basin area and
the Carpathian Foredeep (e.g. Kovač et al., 2003). Tectonic
movements attributed to the Styrian Tectonic Phase (Stille,
1924), as a consequence of plate movements (e.g. Mazzolki
and Helman, 1994) opened the former seaways again by the
end of the early Miocene, leading to extensive middle Mioce-
ne transgressions (Rögl, 1998, 1999). Transgression in the
Central Paratethys occurred as far as the area of Karpatian
sedimentation (Fig. 1; Kovač et al., 2007), extending towards
the Transylvanian and Dacian Basins, to the Carpathian Fore-
deep, and connected with the Eastern Paratethys, which was
also again marine (Fig. 1; Hamor & Halmai, 1988).
The Styrian Tectonic Phase of Stille (1924) characterizes tec-
tonic events at the early/middle Miocene boundary; that is, at
________
Volume 102 2009
KEYWORDS
Badenian Transgressions
Chronostratigraphy
Central Paratethys
Middle Miocene
Styrian Phase
Styrian Basin
The Styrian Basin: a key to the Middle Miocene (Bade-
nian/Langhian) Central Paratethys transgressions___
1)*) 2) 3) 1) 4)
Johann HOHENEGGER , Fred RÖGL , Stjepan ĆORIĆ , Peter PERVESLER , Fabrizio LIRER ,
3) 5) 5)
Reinhard ROETZEL , Robert SCHOLGER & Karl STINGL
1) University of Vienna, Department of Palaeontology, Althanstrasse 14, A 1090 Wien, Austria.
2) Natural History Museum Vienna, Burgring 7, A 1010 Wien, Austria.
3) Austrian Geological Survey, Neulinggasse 38, A 1030 Wien, Austria.
4) Istituto Ambiente Marino Costiero – CNR, Calata Porta di Massa, interno Porto di Napoli, I-80133 Napoli, Italia.
5) University of Leoben, Department of Geosciences and Geophysics, A 8700 Leoben, Austria.
*) Corresponding author, johann.hohenegger@univie.ac.at
the Karpatian/Badenian and Burdi-
galian/Langhian boundaries in the
Central Paratethys and Mediterrane-
an regions, respectively. This pha-
se, as indicated by its name, is de-
fined by the Neogene tectonic his-
tory of the Styrian Basin of SE Aus-
tria, which forms a segment of the
western part of the Intra-Carpathian
Pannonian Basin system. Tectonic
activity was accompanied by exten-
sive volcanism (Ebner and Sachsen-
hofer, 1991; Sachsenhofer, 1996).
Palaeoecological as well as tec-
tonic changes characterize the Kar-
_
patian/Badenian boundary interval, with a general increase in
warm-water species (Badenian climatic optimum) and chang-
ing water depths in regional settings (Harzhauser et al., 2003;
Spezzaferri et al., 2002a, 2004).
One of the problems encountered when correlating the trans-
gression forming the base of the Badenian in the Central Pa-
ratethys area is connected with the biostratigraphical identifi-
cation of the event. Commonly, the main transgression near
the base of calcareous nannoplankton Zone NN5 (Martini,
1971), with co-occurring Praeor bulina circularis and Orbuli-
na suturalis, has been considered to be the basal Badenian
transgression. Due to this coincidence, the Badenian in the
Carpathian area of Romania and also in the Transylvanian
Basin was considered to start with nannoplankton Zone NN5,
subzone NN5a, the Geminithella rotula subzone (Marunteanu
et al., 1999; Chira, 2000). However, in the Mediterranean, the
_______________________
base of the Langhian falls within the
calcareous nannofossil Zone NN4
and has historically been identified
with the first appearance of Praeor-
bulina sicana (Fornaciari and Rio,
1996; Fornaciari et al., 1997). Con-
sequently, some authors correlated
the lowermost Langhian (calcareous
nannofossil Zone NN4) with the Kar-
patian instead with the basal Bade-
nian (e.g. Andrejeva-Grigorovich et
al., 2001).
Work in the Styrian Basin from 2000
to 2006 revealed complex Styrian
Tectonic Phase deformation and
Badenian transgressions. As a re-
sult, it was possible to separate dif-
ferent Badenian transgressive hori-
zons for the first time, especially in
the upper part of the Wagna sec-
tion, and to document what were
previously extended gaps in the se-
dimentation.
In an initial attempt, these problems
____________________
were discussed by comparing the Karpatian/Badenian transi-
tion in the Styrian Basin and in the Molasse Basin of Lower
Austria (Spezzaferri et al., 2002 a,b; Rögl et al., 2005, 2007).
In the Molasse Basin, a distinct clastic Badenian sequence
(calcareous nannofossil Zone NN4 to NN5) lies between the
Karpatian Laa Formation and the early Badenian Grund For-
mation, showing at least two transgression events (Ćorić and
Rögl, 2004). The new implications of repeated Badenian trans-
gressions in the Central Paratethys have been recently consi-
dered by Kovač et al. (2007).
The definition and separation of the Karpatian and Badenian
successions in the investigated sections was made possible
by an evaluation of calcareous nannoplankton, planktonic and
benthic foraminifera and also mollusc associations (Rögl et al.,
2003; Ćorić et al., 2004a,b). As in the Langhian type section,
an overlap of the calcareous nannoplankton Zone NN4 and
__________________________
Alastair M.D. GEMMELL & Christoph SPÖTL
Figure 1: Central Paratethys: palaeogeographic reconstruction of the Early Badenian main trans-
gression within nannoplankton zone NN5 (Rögl and Repp, Naturhistorisches Museum Wien)._______
Figure 2: Styrian Basin: tectonic setting with location of Wagna, Retznei, Katzengraben and the
investigated deep wells (according to Sachsenhofer, 1996)._________________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
the first appearance of Praeorbulina was taken as diagnostic
of the basal Badenian. Spectacular occurrences of molluscs
in the Central Paratethys demonstrate the differences be-
tween the Karpatian and Badenian stages; for examples, 72
gastropod species made their first appearance in the Karpa-
tian, compared to 439 in the early Badenian, whilst for bivalve
taxa the values are 128 species compared to ca. 350, respec-
tively (Harzhauser et al., 2003; Harzhauser and Piller, 2007).
In the present study, the lithological sequences in the Wagna
brickyard and neighbouring Retznei cement quarry, as well as
the Katzengraben section near Spielfeld, have been biostrati-
graphically dated with calcareous nannoplankton and plankto-
nic foraminifera. Preliminary results were given by Lirer et al.
(2006) and Rögl et al. (2005, 2006 a, c). Palaeomagnetic mea-
surements have been correlated with the polarity time scale
_
of Lourens et al. (2004a) and new radiometric ages from the
Styrian Basin (Handler et al., 2006) are discussed. For a bet-
ter understanding of the development in deeper parts of the
basin and in sections with more continuous sedimentation,
some deep wells have been studied in detail (Perbersdorf 1,
Petersdorf 1; Fig. 2).
Foraminifera have been deposited with the Micropalaeonto-
logical Collection of the Natural History Museum, Vienna, while
the calcareous nannoplankton and the Perbersdorf 1 micro-
fossils have been placed at the Austrian Geological Survey,
Vienna. A number of publications have documented the re-
sults produced during the project (Spezzaferri et al., 2001a-c,
2002a-b, 2004; Rögl et al., 2002, 2005, 2006 a-c, 2007; Ćorić
et al., 2004a,b; Hohenegger et al., 2005; Lirer et al., 2006).
Identical sections and sample splits were used by Latal and
Piller (2003) for isotope studies and by Soliman and Piller
(2007) for the investigation of dinoflagellates.
The Styrian Basin, which is part of the western Pannonian
Basin system, has been subdivided by swells into different
subbasins. The main structure, the Middle Styrian Swell, se-
parates the Western from the Eastern Styrian Basin (Fig. 2).
The basement is formed by the Austroalpine nappe system.
Subsidence of the basin, which started during the early Mio-
cene, probably during the Ottnangian, was connected with the
lateral extrusions of crustal wedges along strike-slip faults
towards the Pannonian Basin (Decker and Peresson, 1996;
Frisch et al., 2000). A combination of block rotation, subsiden-
ce and uplift formed the different subbasins. Large areas
were covered by lava flows during extensive volcanic activity.
Extended lignite formation occurred in the Western Styrian
Basin during the early and early middle Miocene, on top of
coarse-grained fan deposits. During the Karpatian, the Para-
tethys Sea transgressed across the Eastern Styrian Basin,
which was comprised of swamp and floodplain deposits of
probably Ottnangian age, resting on a deeply eroded meta-
morphic substratum. Angular unconformities and sedimenta-
tion gaps (Styrian Unconformity) mark the Karpatian/Badenian
boundary. A series of marine transgressions of the Badenian
Sea followed on top of the Karpatian deep-water sediments
(the Steirischer Schlier). In the Styrian Basin, the transgres-
sions reached their greatest extent in the early Badenian.
During the Sarmatian and Pannonian, a continuous shrinking
of the relict sea and lake has been documented (Kollmann,
1965; Flügel and Neubauer, 1984; Ebner and Sachsenhofer,
1991; Sachsenhofer, 1996; Gross et al., 2007; Schreilechner
and Sachsenhofer, 2007).
The sections investigated at Wagna, Retznei and Katzengra-
ben belong to the southern Gnas Subbasin and were strongly
influenced by the development of the Middle Styrian or Sausal
Swell (Fig. 2). Extensive research in this region, with descrip-
tions of outcrops, lithostratigraphic subdivisions, and cyclostra-
tigraphic interpretations were presented by Friebe (1988, 1990,
1991, 1993), Schell (1994) and Holzer (1994).
_________________________________
_____________
_____________________________
____________
2. Geological setting
Figure 3 A-C: a) Wagna, old brickyard: overview with extended
section of the Karpatian "Steirischer Schlier", cut by the “Styrian Un-
conformity” (1), transgre ssed by Badeni an shal low wat er sedi ments
with a patch reef (2), and base of sandstone layers demonstrating dis-
cont inui ty at the Zone NN4/NN5 boundary (3); t he top of t he section
formed by corallinacean limestone of the Weissenegg Formation (4); b)
Retznei , Lafarge- Perlmoo ser cement factory, ma in quarry: sampled
sections (arrows); c) Katzengraben near Spielfeld, outcrop during exca-
vation of the sand pit: the slightly tilted Karpatian “Steirischer Schlier” is
cut by the “Styrian Unconformity” (arrow) and topped by Badenian silts
and sands of the Kreuzberg Formation (photo J.G. Friebe, Dornbirn)._
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Figure 4: Wagna, old brickyard; section 1 sampled in 2000; sections 2 and 3 sampled 2001- 2002._____________________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
Figure 5: a) Karpatian cyclic sedimentation of "Steirischer Schlier" in the old brickyard Wagna; b)
Wagna, upper part of "Steirischer Schlier", channel filling with crystalline pebbles; c) Wagna, “Styrian
Unconformity”, a layer of mudstone pebbles, interbedded in grey silt marks the Karpatian/Badenian
boundary; d) Wagna, Badenian patch reef, intercalated in bioturbated grey silt and fine sand (arrow);
e) Wagna, coral head from the patch reef; f) Wagna, erosive base of stratified sandstone beds with
mollusc casts. Sedimentation gap at the NN4/NN5 zonal boundary.____________________________
3. Lithostratigraphy and Lithofacies
3.1 Wagna, old brickyard
The old brickyard at Wagna is located south of Leibnitz, on
the western side of the river Sulm, on the road to Aflenz. The
section is divided into two parts (Fig. 3a). The lower extended
part belongs to the Karpatian Steirischer Schlier (Kreuzkrum-
pel Formation; Schell, 1994), whereas the upper part shows
the Styrian Unconformity with various Badenian lithologies.
The term Steirischer Schlier is used here instead of the Kreuz-
krumpl Formation of Schell (1994), which generally refers to
Karpatian near-shore deposits. A description of the Wagna
section was recently given by Gross et al. (2007). The palaeo-
magnetic profile of Auer (1996) from this locality was supple-
mented and updated during the research presented here.
Section 1 (samples Wag01–Wag26; Fig. 4), sampled in the
lower part of the former clay pit, comprises mainly Karpatian
Steirischer Schlier, with the Styrian Unconformity lying between
samples Wag23-24 near the top (Spezzaferri et al., 2002a).
Sections 2 and 3, in the upper part of the outcrop, cross the
Karpatian/Badenian boundary and expose the Styrian Uncon-
formity between samples Wag01/16-17 and Wag02/07-08
(Fig. 4).
The exposed 75 m of Steirischer Schlier shows a cyclic se-
___
dimentation of dark-grey, calcare-
ous, silty shales, interbedded by
15-20 cm thick dolomitic limesto-
nes (Fig. 5a). In the upper part of
the Steirischer Schlier, a channel
filling with basement pebbles cuts
the layered succession (Fig. 5b).
The beds show a dip of about 20°
towards 085° E, becoming less in-
clined in the upper part. A slight
angular disconformity, with a thin
pebble layer, separates the shales
from overlying sediments. Above
this disconformity follow 5 m grey,
bioturbated, clayey silts of Karpa-
tian age.
Nannofossil assemblages from
the Steirischer Schlier are rich and
well preserved, dominated by Coc-
colithus pelagicus, Reticulofenes-
tra minuta and Sphenolithus hete-
romorphus. The foraminiferal fau-
na, which has been recrystallized,
is dominated by agglutinated spe-
cies such as Gaudryinopsis bere-
goviensis, Textularia laevigata, Spi-
rorutilus carinatus and Cribrosto-
moides. Among calcareous benthic
foraminifera, large Globobulim ina
pupoides and G. pyrula, together
with Allomorphina trigona, Chilos-
tomella ovoidea and Valvuline ria
complanata indicate dysoxic bot-
tom conditions. The water depth
during deposition of the Steirischer
Schlier has been estimated at be-
tween 225 m and 315 m, with small
variations and a shallowing upward
tendency (Spezzaferri et al., 2004;
Hohenegger et al., 2005; Hoheneg-
ger, 2005). Planktonic foraminifera
are mainly small-sized, five-cham-
bered globigerinas, e.g. Globigeri-
_____________________
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Figure 6: a) Retznei, main quarry; Karpatian section of “Steirischer Schlier” below the carbonate
buildup; b) Retznei, main quarry; base of Badenian carbonate buildup with bored boulders; c) Retznei,
main quarry; outcrop of so-called “Geröllmergel”; d) Retznei, main quarry; detail of Figure 6c: grey
silts and sands with mainly crystalline pebbles, intercalated between Karpatian Schlier and Badenian
carbonate buildup; e) Thalassinoides from Retznei, main quarry, section 2b; f) Flute casts of the base
of the main sandstone layer at section 1, between 22.8 and 24.5 m.___________________________
na ottnangiensis, G. tarchanensis and Turborotalita quinque-
loba. The abundance of agglutinated and sparseness of plank-
tonic foraminifera have been interpreted to be a result of vol-
canic activity in the Styrian Basin (Spezzaferri et al., 2002a).
The top of the Karpatian shales is marked by a distinct ero-
sional and angular unconformity, with reworked silty clasts of
Steirischer Schlier in the pebbly mudstone of the Geröllmergel
(Fig. 5c) and small oysters, followed by 3-5 m of bluish-grey,
sandy silts. The foraminiferal fauna, as well as shallow-water
ostracods and bivalves, mark this distinct unconformity. A
strong change from deep-water assemblages of about 250 m
water depth to inner neritic depths (< 50 m) characterizes this
Styrian Unconformity that here encompasses the Karpatian/
Badenian boundary and the Bur5/Lan1 sequence boundary
_
(Rögl et al., 2002; Spezzaferri et
al., 2002 a). The nannoflora of Zo-
ne NN4 in these sandy silts shows
a strong increase in Helicosphaera
ampliaperta. Foraminiferal assem-
blages are corroded and dominated
by Ammonia and elphidiids. The first
Praeorbulina sicana occurs, as well
as abundant small globigerinids.
The following ca. 2.5 m of grey,
bedded sandy limestone (dip 5° to-
wards 015° E) contains a high am-
ount of skeletal debris. In section
3, these beds interfinger laterally
with a small patch reef (Wag02/15
to Wag02/16, Fig. 4), different from
the succession in the Weissenegg
Formation (Figs 5d, e). The follow-
ing horizon is characterized by bio-
turbated, greyish, micaceous san-
dy silts and silty sands, interrupted
by a thin concretion layer, and with
fragments of thin-shelled bivalves
at the base. The first Praeorbuli-
na glomerosa occurs on top of the
patch reef.
These beds are overlain by ca. 3
m of rhythmically stratified brow-
nish silty sandstone and siltstone
layers with erosive bases and with
abundant mollusc casts (Fig. 5f).
The erosive base of the lowermost
sandstone bed (above Wag02/19,
Fig. 4) encompasses the NN4/NN5
boundary, thus indicating a distinct
sedimentation gap. Foraminifera
are mostly dissolved, but the first
record of Amphistegina mammilla,
typical of the Badenian has been
observed. Praeo rbulina circularis
and Orbuli na suturali s also have
___
___________________
their first occurrences here.
A lithostratigraphic definition of the clastic sequence between
the Steirischer Schlier and the corallinacean limestones of the
Weissenegg Formation (see below) is missing, probably also
due to former biostratigraphic misinterpretations of the Karpa-
tian/Badenian boundary (e.g. Latal and Piller, 2003). A corre-
lation with the Kreuzberg Formation (Friebe 1990) has to be
checked, as this formation interfingers with the younger Weis-
senegg Formation. The Geröllmergel of Retznei at least partly
corresponds to this clastic sequence.
The top of the section consists of ca. 7 m of layered coralli-
nacean limestone with intercalated silty marls of a carbonate
buildup, the Weissenegg Formation (Friebe, 1990). This marks
a distinct facies change, with a clear sedimentary discordance
___________________________
____________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
and erosive base to the underlying sandstones. In the marly
layers, a rich foraminiferal fauna, with agglutinated tropical/
subtropical shallow water species, such as Pseudogaudryina
lapugyiensis, P. sturi and Paragaudryinella interjuncta and al-
so common Amphistegina, occur together with planktonic spe-
cies of Globigerinoides , Praeorbulina and Orbulina. The calca-
reous nannoplankton belong to the nannoplankton Zone NN5.
Dinoflagellate cysts from these sections were studied by So-
liman and Piller (2007). The occurrence of Nematosphaerop-
sis labyrinthus as an indicator of deep water in the Karpatian
confirms results based on benthic foraminifera whilst a num-
ber of thermophilic species point to subtropical conditions
throughout the sections. The position of the Karpatian/Bade-
nian boundary proposed by Soliman and Piller (2007) is not
in agreement with our observations. The correct position of
the boundary in section 1 of Soliman and Piller (2007), which
is based on the sections presented here, lies between sam-
ples Wag23 and Wag24, in section 2 between Wa01/16 and
Wa01/17, and in section 3 between Wa02/07 and Wa02/08
(Fig. 4). The change of dinocyst assemblages was connected
to a change in the palaeoenvironment reflected in the litholo-
gical change in the upper part of the Steirischer Schlier.
The Wagna section continues to the south and is exposed in
the Lafarge-Perlmooser cement quarries in Retznei. Depen-
ding on the relief, some Karpatian shales and relics of clastic
basal Badenian sediments below the corallinacean limestone
are exposed here.
Two outcrops were noted by Friebe (1988, 1993) as Geröll-
mergel. This small, 4 m high first outcrop lies in the middle of
the quarry and exposes Steirischer Schlier (Fig. 6a) and the
eroded top of the Karpatian. The Steirischer Schlier consists
of dark-grey, silty, calcareous shales with sparse pebbles from
the basement. Another pebble layer, containing calcareous
clasts bored by bivalves and with trace fossils (Gastrochae-
nolites; Fenninger and Hubmann 1997), forms the base of a
huge carbonate buildup (Fig. 6b). The nannoflora and micro-
fauna of this short section are similar to the upper part of the
Karpatian in Wagna. The calcareous nannoplankton compri-
ses small reticulofenestrids; the agglutinated foraminiferal spe-
cies Spirorutilus carinatus (Spezzaferri et al., 2002a) is cha-
racteristic. Elsewhere, the dark grey shales contain a typical
Karpatian microfauna with Gaudryinopsis beregoviensis and
Cribrostomoides, together with small calcareous benthic and
planktonic foraminifera.
The second outcrop (Friebe 1988, 1993), which lies further
to the north, exposes Karpatian Steirischer Schlier, Geröllmer-
gel and the base of the carbonate buildup (Fig. 6c). The Kar-
patian is overlain by a pebble layer, followed by 1 to 4.5 m
(Fenninger and Hubmann, 1997) of silt and micaceous fine
sand with mainly basement pebbles (Geröllmergel; Fig. 6d).
____
___________________________________
_______________________________
3.2 Retznei, Lafarge-Perlmooser cement
quarries
3.2.1 Hauptstock, main quarry
The sediment contains some mollusc and echinoid debris,
and a rich foraminiferal and ostracod fauna. Shallow water
species of Ammonia and Elphidium have been transported or
reworked. Pseudogaudryina, Textularia, Uvigerina, Heterolepa,
Cibicidoides and lagenids indicate an inner shelf environment.
This fauna and the planktonic assemblage with Globigerino-
ides trilobus, G. quadrilobatus, Praeorbulina glomerosa and
the nannoplankton of zone NN 5 indicate a correlation with
the clastic Badenian part of the Wagna section below the car-
bonate buildup.
The carbonate buildup of the Weissenegg Formation starts
in the main quarry (Fig. 6b) with a small coral reef and ex-
tends into corallinacean limestones (Leithakalk; Friebe, 1988,
1990). Towards the southeast, the limestones show a basin-
ward transition into reworked material of the reef slope facies.
Marly sands and silts, with tuffitic intercalations, drowned the
top of the buildup and carbonate sedimentation ended after
the start of intense volcanic activity. A thick tuff layer with
black biotite and sanidine is present on top of the limestones.
This layer was recently radiometrically dated to 14.21 ± 0.07
Ma or 14.39 ± 0.12 Ma (Handler et al. 2006).
The section above the carbonate buildup investigated (samp-
led in two overlapping sub-sections, Fig. 7) lies in the south-
eastern part of the main quarry (Fig. 3b). The lower part com-
mences with 5 m of corallinacean limestones of the Weissen-
egg Formation, of which the base is not exposed. Approxima-
tely 8 m of silty clay and silt-clay that contains several tuffitic
intercalations follow above an erosional surface (Fig. 7, sam-
ple R 01/07). The following 45 m show mostly bioturbated,
homogeneous greenish-grey silty clays with intercalated hori-
zons of silty fine sands and silty sands. The pelitic sediments
frequently contain plant remains, molluscs, echinoids, crus-
taceans and fish teeth. The sandy horizons mostly show an
upwards fining and bioturbation (Thalassinoides, Ophiomor-
pha; Fig. 6e). Additionally, a 1 m thick sandstone layer, depo-
sited about 18 m above the top of the limestones (R 01/28
and R 01/29), shows flute casts at its base (Fig. 6f).
The rich foraminiferal fauna of the Lower Lagenidae Zone
assemblages points to an upwards deepening in the section,
from 150 to 300 m water depths, indicating strong subsidence
(Hohenegger et al., 2005). Praeorbulina circularis and Orbuli-
na suturalis occur throughout the section. The nannoplankton
assemblages point to the Helicosphaera waltrans biohorizon
within zone NN5 (Ćorić et al., 2007). This datum conforms to
the recently proposed data in the Mediterranean area (Di Ste-
fano et al., 2008). The dinoflagellate cysts of the siliciclastic
sequence were studied by Soliman (in Gross et al. 2007). The
occurrences of Cerebrocysta poulsenii, C. placacanthum, Ha-
bibacysta tectata and Unipontidinium aquaeductum indicate a
middle Miocene age.
A detailed description of the Rosenberg quarry (new Retznei
quarry) was given by Gross et al. (2007). As before, Badenian
sedimentation starts on top of the Styrian Unconformity with a
_____________________________________
_____________
________
_________________________________
3.2.2 Rosenberg quarry
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Figure 7: Retznei, Lafarge-Perlmooser cement factory, old main quarry; sampled sections with position of investigated samples; in section 1 deep-
water silts and marls with two layers of intercalated tuffites top the corallinaceen limestone of the Weissenegg Formation._______________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
Figure 8: Katzengraben near Spielfeld; sampled section with lithology and stratigraphy._______
layer of coarse pebbles (Basalkon-
glomerat – Geröllmergel). The over-
lying carbonate complex (Erhart and
Piller, 2003) is heterogeneous, but
also starts with coral growth. Fine-
grained calcareous sandstones with
corallinacean debris and Planostegi-
na, the Aflenz Stone (a well-known
building stone of the region), overlie
coral patchreefs. Corallinacean lime-
stones and patches of corals form
the upper part of the carbonate build-
up. The occurrence of Planostegina
giganteoformis is characteristic for
the Lower Badenian in the Styrian
Basin. An erosional surface trunca-
tes the limestones, followed by a si-
liciclastic sequence, reflecting increa-
sing water-depths.
A stratigraphic succession, compa-
rable to the Wagna and Retznei sec-
tions, but with a more clastic cha-
racter, is exposed in the abandoned
sand pit at Katzengraben west of
Spielfeld (Figs 2, 3c). The >22 m
high section consists of silt with fine
sand layers and lenses; layers of
medium sand are present in the ba-
sal section and clean, sometimes
concretionary sandstone is charac-
teristic of the upper part (Fig. 8). Co-
arse gravels and fine gravel hori-
zons occur within a silt layer expo-
sed from 5.35 to 6.20 m above the
present base of the outcrop. At the
base of these gravel bearing silts, a
layer of reworked Karpatian shale
pebbles was also observed. From
11.5 to 11.80 m, a silty fine sand lay-
er with fine gravels contains disper-
sed lonestones on its top. Besides
very rare mollusc shell fragments in
the higher fine sandy part, the Kat-
zengraben section is free of macro-
fossils. Trace fossils such as Plano-
lites, Thalassi noides and Scolicia
mainly occur in the upper part of the
section.
The Kreuzkrumpel Formation was
defined from Karpatian deposits in
the southwestern part of the Gam-
litz embayment (Schell 1994). This
______________
____
3.3 Katzengraben sec-
tion near Spielfeld
formation, which is unpublished (and thus invalid), encompas-
ses silty calcareous shales (Steirischer Schlier), with interbed-
ded sands, sandstones and gravel layers. Friebe (1990) des-
cribed the Badenian sands and gravels in this area as the
Kreuzberg Formation.
Friebe (1993), who described the Katzengraben outcrop with
the Styrian Unconformity (Fig. 3c), regarded the lowermost
part of the transgressive sequence with sandy conglomerate
and siltstone cobbles as Karpatian. However, based on our
observations, this part of the succession should be correlated
with the sediments characteristic of the first Badenian trans-
gression in the Wagna section (Fig. 4: Wag02/08 to Wag02/
19). In both places, Karpatian shale cobbles mark the base of
Badenian, accompanied by a distinct change from deep-water
to shallow-water deposits. Friebe (1993) noted fossil debris,
with oysters and Gastrochaenolites-borings, indicating shal-
low-water conditions. The occurrence of glauconite in the pro-
posed Badenian sands confirms an environmental change to
warmer and shallower conditions, as pyrite is a common com-
________________________________
ponent in Karpatian sediments. Hol-
zer (1994) correlated the Karpatian
shales with the Kreuzkrumpl Forma-
tion and the sediments above the
angular unconformity with the Weis-
senegg Formation. The conglome-
rate bed in the higher part (ca. 12
m) of the sand succession (Fig. 8)
corresponds to another disconformi-
ty and a further Badenian transgres-
sion, as demonstrated by calcare-
ous nannoplankton and foraminifera.
Planktonic species of Praeorbulina
and Orbulina were not recorded. The
Karpatian/Badenian boundary is mar-
ked by the first occurrence of the
stratigraphically important shallow
benthic foraminiferal species Colo-
minella paalzowi and Lingulina cos-
tata and the overlying disconformity
by the occurrence of Vaginulina le-
gumen and Pseudogaudryina lapu-
gyensis. The calcareous nannoplank-
ton flora is similar to associations in
the Wagna section, showing both an
assemblage change within Zone NN4
at the Karpatian/Badenian boundary
and the NN4/NN5 boundary at the
base of the Badenian conglomerate,
with the occurrence of H. waltrans.
The mass occurrence of the small
planktonic foraminiferal genus Cassi-
gerinella in both Karpatian and Ba-
denian (reworked?) sediments is in-
teresting, as this was not observed
in the Wagna section.___________
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
3.4 Perbersdorf 1 deep well
In the southern Styrian Basin (southern Gnas Subbasin), a
deep well at Perbersdorf (Fig. 2) was fairly continuously cored
for scientific research in 1953, by the R.K. van Sickle Company
(material deposited at the Austrian Geological Survey). The suc-
cession shown in Table 1 is based on Kapounek (1954). Vol-
canic layers and tuffites are common, especially below 600 m
drilling depth.
The results were reported by Kapounek (1954) and Kollmann
(1965), partly revised by Rögl et al. (2002) and Spezzaferri et
al. (2004). The well ended in Palaeozoic phyllites. Although
Spezzaferri et al. (2004) placed the Karpatian/Badenian boun-
dary at 501 m depth, at the highest occurrence of Uvigerina
graciliformis, subsequent research, also based on calcareous
nannoplankton, showed that the Badenian started much lower.
The important Badenian nannoplankton marker horizon of H.
waltrans was found between 304 m and 370 m, with the nan-
noplankton zonal boundary NN4/NN5 placed at 501 m, accom-
panied by a disconformity. Typical Karpatian nannoplankton
_______________________________________
Table 1: Perbersdor f 1 deep well; lithology and revised biostratigr aphy of the deep well in the
southern Gnas Subbasin._____________________________________________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
Table 2: Petersdorf 1 deep well; lithology and bi ostr atig raph y of the deep well in the northern
Gnas Subbasin.____________________________________________________________________
assemblages of NN4 were observed between 862.0 m and
930.8 m. Planktonic foraminiferal assemblages in the lower
part of the section are dominated by Globigerina s.l., but index
species are very rare. The first occurrence of Praeorbulina cf.
sicana was in the upper part of the section at 442 m. Only ve-
ry rare Globigerinoides were found down to 800 m. In the dee-
per parts of the well, agglutinated assemblages with a domi-
nance of Bathysiphon alternate with rich calcareous benthic
faunas. Occurrences of Uvigerina macrocarinata and Vaginul-
ina legumen indicate an early Badenian age. Based on this and
the well-log, the base of the Bade-
nian has been placed at 838 m.
The Karpatian sediments show fo-
raminiferal assemblages similar to
the Badenian, with abundant ag-
glutinated species. No sedimentary
break or distinct faunal change was
observed. The lowermost investiga-
ted sample, at 927.8 m, has a well-
developed foraminiferal fauna with
common Spirorutilus. This indicates
sedimentation at water depths grea-
ter than those in the sublittoral fa-
cies. Coastal or near-shore Karpa-
tian sediments are missing. Marine
Karpatian sediments were only do-
cumented from 838 to 935 m.
Dark grey to red brown shales with
layers of conglomerates and tuffites
form the lower part of section, with
some traces of lignite. The microfos-
sil content is reduced to silicified
stems and tubes, probably of plant
roots. This lower part of the section
is subdivided into two parts. The
upper part (935 – 1335 m) is domi-
nated by conglomerates and dark
shales that might be correlatives of
limno-fluviatile Ottnangian deposits
(the lower Eibiswald Formation of
Kollmann, 1965). The lowermost part
(1335 – 1470 m), with reddish, gree-
nish and black shales and red brec-
cias corresponds to the continental
?Ottnangian Limnic Series. Kapou-
nek (1954) reported some fragments
of terrestrial gastropods from these
shales. The sediments lie unconfor-
mably on the metamorphic base-
ment. The core ended at 1477 m,
in Palaeozoic phyllites.
The Petersdorf 1 deep well was
drilled in 1995 by the Rohöl-Aufsu-
chungs AG (Vienna) in the northern
Gnas Subbasin (Fig. 2), penetrating
mainly coarse clastics of Pannonian
und Sarmatian age. A complete Ba-
__
____
________-__
3.5 Petersdorf 1 deep
well
denian succession was drilled down to 2127 m (Tab. 2). A
bloom of Orbulina was observed at 1470 – 1490 m; this oc-
curs in the lower Badenian of the Styrian Basin at many drill
sites. Only scarce microfossil assemblages were observed
between 1673 m and 1867 m, probably due to volcanic acti-
vity. Index fossils are rare below 2030 m, while agglutinated
foraminifera are more common. The Karpatian part comprises
the section from 2127 m to 2342 m. A core was taken from
2308 m to 2318 m, from which thin-sections showed dark
grey-brown, bioturbated shales with rare agglutinated tubes.
The core samples were barren of micro- and nannofossils.
Conglomerates with intercalated shales, sandstones and some
tuffites were found from 2342 m to 2901 m. This sequence
can be correlated with the limno-fluvial Ottnangian deposits in
other wells. The well ended at 3084 m in Palaeozoic micace-
ous slates.
The Übersbach deep well 1 was drilled in 1958/1959 by the
Rohöl-Aufsuchungs AG (Vienna) in the Fürstenfeld Subbasin
(Fig. 2). A profile and detailed description was given by Koll-
mann (1965: Pl. 3); this is presented here in short form (Fig.
9). From 8 m to 209 m, Pannonian gravel, sand and calcare-
ous clay were drilled, followed by Sarmatian clays, oolites,
sand, and gravel down to 1023 m, with a discordance and gap
to the Upper Badenian Bulimina-Bolivina Zone. Calcareous clays
_________________________________________
3.6 Übersbach 1 deep well
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Figure 9: Correlation of deep wells in the Styrian Basin: differences of subsidence in different
subbasins..The Karpatian marine sedimentation ended at the Styrian Unconformity, followed by the
Badenian transgression. A basal Badenian conglomerate is developed in the Fürstenfeld Subbasin
(Übersbach 1).______________________________________________________________________
with sandstones, corallinacean lime-
stones and some tuffites form the
Badenian succession, which trans-
gressed with a basal conglomerate
at 1582 m. Rich microfossil assem-
blages belonging to the Lagenidae
Zone appear in the Lower Badenian,
with a first occurrence of Orbulina.
Marine Karpatian sandstones, calca-
reous shales and tuffites were recor-
ded between 1582 m and 1980 m.
Trace fossils, a few bivalves and a
poor microfauna were observed, do-
minated by agglutinated foraminife-
ra. Index species are missing; only
a few Ammonia and Elphidium oc-
cur in the lowermost part. The un-
derlying sequence consists of sand-
stones, conglomerates and shales
with some lignite seams. This part
of the sequence is considered to be
non-marine, and therefore correla-
ted with the limno-fluvial Ottnangian,
in contrast to the interpretations of
Ebner and Sachsenhofer (1991) and
Polesny (2003). Flood-plain deposits
with red loam, coal seams and bi-
tuminous marls at the base (Limnic
Series) are considered to be Ottnan-
gian (Polesny, 2003) but terrestrial gastropods and plant fos-
sils did not allow a precise biostratigraphic determination. The
basement, at 2636 m, is formed by Palaeozoic banded lime-
stones.
The deep geothermal well at Fürstenfeld was drilled in 1984/
1985 in the Fürstenfeld Subbasin (Fig. 2). Friebe and Poltnig
(1991) published a lithological and biostratigraphic subdivision
of the well (Fig. 9). Early Pannonian sediments were drilled
down to 194.5 m. Sarmatian sediments containing the basal
Anomalinoides Zone followed, down to 1330 m. The Badenian
succession was difficult to subdivide; based on other, nearby
wells, it was here assumed that the lower part of upper Bade-
nian correlates with the zone of agglutinated foraminifera and
that the boundary of the middle/lower Badenian should be
placed at 1690 m. In contrast to Friebe and Poltnig (1991)
and Polesny (2003), we have placed the Karpatian/Badenian
boundary at 2620 m, based on the occurrence of Praeorbu-
lina glomerosa. The Karpatian, rich in conglomerates (2620 –
2748 m), yielded Globigerinoides bisphericus. The well ended
at 3145 m in Palaeozoic rocks. Limno-fluviatile, coarse-clastic
?Ottnangian sediments were missing in this well.
Biostratigraphic problems of the early/middle Miocene, Kar-
3.7 Fürstenfeld Thermal 1 deep well
4. Biostratigraphy
__________
ricus in the upper part (Cicha and Rögl, 2003). The upper sur-
face of the Karpatian was commonly an erosion surface in
Austrian Neogene basins. The base of the Badenian is deter-
mined by the first appearance of the planktonic foraminiferal
genus Praeorbulina. This boundary is correlated with the Bur-
digalian/Langhian boundary in the Mediterranean region. There-
fore, the basal early Badenian still belongs to nannoplankton
Zone NN4 (Ćorić et al., 2004a).________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
Figure 10: Wagna, old brickyard, section 3. Interpreted stratigraphy, combining lithology, biostra-
tigraphy and palaeomagnetic results. The Styrian Unconformity is interpreted to corresponds to the
Bur5/Lan1 sequence boundary. The intra-Badenian discontinuity at the Lan2/Ser1 sequence boundary
separates a first Badenian transgression from the Central Paratethys wide Badenian main transgres-
sion. At the base of the corallinacean limestone of the Weissenegg Formation an additional sedimen-
tation gap is observed._______________________________________________________________
The historical method to identify
the base of the Langhian is repre-
sented by the first evolutionary ap-
pearance of Praeorbulina glomero-
sa. Fornaciari et al. (1997) propo-
sed a revision of the Langhian his-
torical stratotype, suggesting that
the base of the type Langhian pre-
dates the H. ampliaperta LO and
contains Sphenolithus heteromor-
phus, hence falling within Zone NN4
of Martini (1971), whilst the first evo-
lutionary appearance of P. glomerosa
occurs about 100 meter below the
base of the Cessole Marls, which
historically indicate the base of the
Langhian (Vervloet 1966). Moreover,
Gelati et al. (1992) considered the
Langhian stratotype to represent a
single depositional sequence, corre-
rd
lated to the 3 -order cycle 2.3, su-
percycle TB2, of the Global Cycle
Chart of Haq et al. (1988).
Recently, Lourens et al. (2004a) pro-
posed, but without a formal definition,
placing the base of the Langhian,
and therefore the early/middle Mio-
cene boundary, at the top of chron
C5Cn, dated at 15.974 Ma.
At present, the available published
data clearly indicate that there is no
general agreement for the identifi-
cation of the base of the Langhian.
Moreover, the poorly preserved ma-
rine Langhian records prevent a clear
identification of the Globigerinoides-
Praeorbulina lineage, which is al-
ways used to identify the base of
the Langhian.
In Appendix 2 of Lourens et al. (2004
b), the first appearance of P. glome-
rosa is given at 16.27 Ma, which is
in full agreement with the former usa-
ge. Therefore, we conti-nue to use
this biostratigraphical marker, in com-
bination with the base of the polarity
chron C5Cn.1r at 16.303 Ma, as the
_______
_______
_________________
patian/Badenian boundary in the Central Paratethys and cor-
relations with Mediterranean stages were recently discussed
in detail (Rögl et al., 2002, 2007; Ćorić et al., 2004a, b). The
Karpatian stage is characterized by the first appearance of
the benthic foraminifer Uvigerina graciliformis within nanno-
plankton zone NN4, defined as the interval between the LO of
Sphenolithus belemnos and the LO of Helicosphaera amplia-
perta, as well as by the appearance of Globigerinoides bisphe-
base of the middle Miocene (Langhian) and, consequently, as
the base of the Badenian.
In the Central Paratethys and the Styrian Basin, the Steiri-
scher Schlier belongs to the Karpatian, due to the occurrence
of G. bisphericus and the marker of the calcareous nanno-
plankton zone NN4, H. ampliaperta. The Karpatian benthic
foraminiferal marker Uvigerina graciliformis is also common
here. In most sections, the topmost part of the Steirischer
Schlier has been eroded and thus the marker species, G. bis-
phericus, is not well represented.
For stratigraphical subdivisions based on nannoplankton, the
marker species H. ampliaperta and S. heteromorphus have
been used; zone NN5 is defined by the absence of the former
and presence of the latter. Karpatian and the lower part of the
Badenian sediments in Wagna, Katzengraben und Retznei can
be assigned to nannoplankton Zone NN4, whereas the upper
part of the lower Badenian belongs to NN5.
Helicosphaera waltrans (Theodoridis, 1984) can be used as
an additional marker within the S. heteromorphus Zone (NN5),
by defining the LO of this species as the upper boundary of
the H. waltrans subzone. The importance of this short range
species was recognized by Fornaciari et al. (1996), but was
not used as a marker for the subdivision of the miocene Medi-
terranean nannofossil zonation. H. waltrans was described by
Švábenická (2002) and Ćorić and Švábenická (2004) from
middle Miocene localities in the Central Paratethys (Vienna
Basin and Alpine-Carpathian Foredeep). Recently, the Last
_____________________________
_______________________
_______________
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Figure 11: Palaeomagnetic results and interpretation of chrons from the Retznei Lafarge-Perl-
mooser cement factory, old main quarry and new quarry Rosenberg (Stingl and Scholger 2005).____
Common Occurrence (LCO) of this
form was used by Di Stefano et al.
(2008) for the subdivision of the Sphe-
nolithus heteromorphus Interval Zo-
ne (MNN5) and for defining the up-
per boundary of the Sphenolithus he-
teromorphus – Helicosphaera wal-
trans Subzone (MNN5a). Abdul Aziz
et al. (2008) dated the short range
of this form, with the First Common
Occurrence (FCO) at 15.476 Ma and
the LCO at 14.357 Ma (interpolated
to ATNTS 04).
A subdivision of the Badenian in the
Styrian Basin similar to the ecostrati-
graphic zonation of Grill (1941, 1943)
for the Vienna Basin, is problematic,
especially for the early Badenian. The
revision of this zonation by Papp and
Turnovsky (1953) was based on Uvi-
gerina lineages; this subdivided the
early Badenian successions by the
range of U. macrocarinata into the
Lower and Upper Lagenidae Zones.
In the Styrian Basin, this species ran-
ges throughout the early Badenian
because of a distinctly deeper envi-
ronment, where heavily costate Uvi-
__________-_______
gerina species dominate. Markers of the early Badenian in the
deep basin are represented by Vaginulina legumen, large len-
ticulinas (e.g. Lenticulina ariminensis, L. orbicularis), together
with U. macroc arinata, and sometimes replace the missing
Praeorbulina. In shelf areas, agglutinated species such as Co-
lominella paalzo wi, Psammolingulina papillosa, Pseudogau-
dryina lapugyensis, P. sturi and Paragaudryinella interjuncta
mark the climatic change to warmer conditions at the base of
the Badenian by their first occurrences. In the deep wells of
the Styrian Basin, a bloom of Orbulina has been observed in
the upper part of the lower Badenian, probably still in the Lo-
wer Lagenidae Zone.
In the investigated sections, a biostratigraphic subdivision of
Karpatian and Badenian sediments and a correlation between
shallow and deep water regions can be demonstrated:
Here, only the upper part of the section, with the Styrian Un-
conformity and the Badenian part (Fig. 10) is discussed, be-
cause Spezzaferri et al. (2002a, 2004) gave detailed analyses
of the Karpatian part.
The Karpatian and Badenian sediments from section 1 (Fig.
4, App. 1a) and section 2 (Fig. 4, App. 1b) contain Helicos-
phaera ampliaperta, which defines nannoplankton Zone NN4.
Most of section 3 (Wag02/01 to Wag02/19), including the Sty-
rian Unconformity, contains similar nannoplankton assembla-
ges as the samples from sections 1 and 2 (App. 1c). There-
________________________________
______
________________________________
4.1 Wagna, former clay pit
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
fore, this part of section 3 can be assigned to the same nan-
noplankton zone. The last occurence of H. ampliaperta was
observed in sample Wag02/19 and thus the NN4/NN5 boun-
dary can be placed between samples Wag02/19 and Wag02/
20, on the erosive base of the lowermost sandstone bed. Sil-
ty marls from the uppermost part of section 3 (Wag02/20 to
Wag02/25) contain very rich nannoplankton assemblages, in-
cluding Helicosphaera waltrans and can thus be attributed to
Zone NN5. Just above the angular discordance and clay-peb-
ble layer, the planktonic foraminifer Praeorbulina sicana marks
the base of the middle Miocene (base Badenian) in sample
Wag 02/09 (Fig. 4), followed by Praeorbulina transitoria and
P. glomerosa. In one of the weakly cemented samples be-
tween the sandstones, Praeorbulina circularis is recorded to-
gether with Orbulina suturalis. Starting with the corallinacean
limestones near the top of the Wagna section, a rich plankto-
nic assemblage with co-occurrence of Praeorbulina and Orbu-
lina is observed. In this upper part of the Wagna section, a ty-
pical early Badenian benthic foraminiferal fauna appears also
(Apps 1d, e).
A small outcrop of the Steirischer Schlier (Fig. 6a) was in-
vestigated by Spezzaferri et al. (2002a) in the Retznei quarry.
Calcareous nannoplankton constrain the age of these sedi-
ments to zone NN4; the appearance of U. graciliformis with-
out Praeorbulina is indicative for the Karpatian. The upper-
most, Badenian part of this section yielded nannoplankton
assemblages with H. waltrans, indicating nannoplankton zone
NN5 (App. 1f). Thus in this section, the Karpatian/Badenian
and the NN4/NN5 boundaries coincide, indicating a sedimen-
tation gap that extended for more than 1 Ma. In the second
outcrop, the foraminiferal fauna of the Geröllmergel lying
above the Steirischer Schlier (Fig. 6c) contains Praeorbulina
glomero sa and Amphistegina mammilla, the latter being a
benthic marker not represented in the Karpatian. The nanno-
flora of these sands and silts belong to zone NN5, with H. wal-
trans. The lower part of this section, in the Steirischer Schlier,
contains H. ampliaperta and can be assigned to zone NN4.
In the Badenian part of the main quarry at Retznei (Fig. 7),
the nannoplankton zone NN5 is recorded throughout the sec-
tion and belongs to the Helicosphaera waltrans horizon (Apps
1g, h). Benthic assemblages correspond to the typical fauna
of the Lagenidae Zone, with Uvigerina macrocarinata, Vaginu-
lina legumen and Amphistegina mammilla (App. 1i). Praeor-
bulina circularis and Orbulina suturalis occur together in both
the basal marls and the corallinacean debris, topping the au-
tochthonous corallinacean limestone. Of stratigraphic impor-
tance are the occurrence of the globorotaliids Paragloborotalia
siakensis/acrostoma and Globorotalia transsylvanica (App. 1j).
The regular occurrence of H. ampliaperta in marly sediments
from the lower part of the section at Katzengraben (Fig. 8: A01
to B02) indicates nannoplankton Zone NN4 (App. 1k). The
_______________________________________
__
4.2 Retznei, main quarry
4.3 Katzengraben
NN4/NN5 boundary has been placed between samples B02
and B03. Note that the rare occurrence of H. ampliaperta in
sample C1/01 probably results from reworking. The upper part
of the section (B03 to C2/1) contains H. waltrans and can be
placed into the lower part of zone NN5. Sphenolithus hetero-
morpus is rare. High percentages of Helicosphaera carteri in-
dicate a shallow-water palaeoenvironment.
A rich foraminiferal fauna was determined in marly samples
of the Karpatian section part. Tests were commonly corroded
and some transportation from shallower regions was recorded
(e.g. Amphistegina, Elphidium). Particularly remarkable are
floods of the small planktonic species Cassigerinella boude-
censis and C. globulosa. Most globigerinas (e.g. Globigerina
falconensis, G. ottnangiensis, G. pseudociperoensis, G. sub-
cretacea) are small and Globoturborotalita connecta, Globige-
rinella cf. regularis and Globoquadrina langhiana also occur.
Small microperforate genera (Tenuitella, Tenuitellinata, Tur-
borotalita) are common. The index fossil Globigerinoides bis-
phericus was observed in sample Katz 1 (Fig. 8). Some ag-
glutinated species, such as Haplophragmoides laminatus, Re-
ticulophragmium karpaticum and Cyclammina karpatica indi-
cate greater water depths (outer shelf). The main fauna con-
sists of calcareous species, where the following uvigerinids
and bolivinids are stratigraphically important: Uvigerina graci-
liformis, U. pygmoides, U. cf. bulbacea, Pappina primiformis,
P. breviformis, Bolivina hebes and B. matejkai.
No distinct faunal change was observed in the Badenian sam-
ples above the main unconformity. Cassigerinella dominates
the planktonic assemblages but the benthic assemblages of
the marly samples are highly diverse. The first typical Bade-
nian immigrants, for example the agglutinated shallow water
species Colominella paalzowi, Pseudogaudryina mayeriana,
together with Bolivina scalprata muscosa and B. viennensis,
occur in sample Katz 3. In sample B 02, the species Uvigeri-
na macrocarinata indicates the Lower Lagenidae Zone. In the
upper part of the Badenian section (samples B 03 to C 1/1)
Pseudogaudryina lapugyensis, P. sturi, Lingulina costata, Pla-
nularia dentata, Planostegina costata and Vaginulina legumen
occur first. The planktonic assemblages are still of small size,
Cassigerinella is common but may have been reworked from
the lower part of the section. The stratigraphically important
genera Praeorbulina and Orbulina have not been observed.
Sediments from the lowermost part (947 m – 1311 m) do not
contain nannofossils (App. 1l). As Helicosphaera ampliaperta
is abundant in samples between 520 – 523 m, the NN4/NN5
boundary has been placed at the disconformity at 501 m. Due
to the absence of this marker species, the upper part of the
section (246 m to 496 m) can be assigned to nannoplankton
Zone NN5. Calcareous nannoplankton assemblages with H.
waltrans were observed from 299 m to 370 m. Abundant small
reticulofenestrids within the nannoplankton assemblages above
the last occurrence of H. ampliaperta confirm this stratigraphic
subdivision.
_______________
____________
__
4.4 Perbersdorf 1 deep well
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Figure 12: Bio-chrono-magnetostratigraphic correlation between Wagna, Retznei
and DSDP-Site 372 (Aziz et al., 2008; Di Stefano et al. , 2008) records. Quantit ative
distribution pattern of Paraglob orotalia siakensis from DSDP-Site 372 (Di Stefano et al.,
2008) and from Retznei (this work). The palaeo-environment of the lower part in the Retznei section was too shallow for P. sia-
kinensis, only in the upper section part the estimated palaeodepth of 250 to 300 m (Hohenegger et al., 2005) was convenient
explaining abundance peaks.______________________________________________________________________________
Foraminiferal assemblages vary in this section strongly in
abundance as well as in composition. All investigated core
samples from 216 to 838 m belong to the early Badenian. A
rich planktonic assemblage, with O. suturalis, P. circularis, P.
sicana and Paragloborotalia siakensis, is present only in the
uppermost part (down to 376 m; App. 1m). At 247 – 248 m,
the marker horizon with the Orbulina bloom was observed. In
the deeper parts, in which there is an increase of volcaniclas-
tic intercalations, the biostratigraphic subdivision depends
mainly on calcareous nannoplankton. Agglutinated foraminife-
ra dominate down to 750 m, followed by rich assemblages of
globigerinas and calcareous and agglutinated benthics. Ben-
thic species such as Vaginulina legumen and U. macrocari-
nata indicate a Badenian age (App. 1n). In contrast to earlier
interpretations (Kollmann, 1965; Spezzaferri et al., 2004), nan-
noplankton and foraminifera indicate that the Karpatian/Bade-
nian boundary must be placed at 838 m. No distinct assem-
blage change could be observed at the boundary and thus
continuous sedimentation may have occurred in this deeper
part of the basin. Rich assemblages of globigerinas and ben-
thic species occur in the Karpatian part of the section (838 –
935 m), with U. graciliformis as the only marker species.
At Petersdorf, the well-log and foraminiferal assemblages indi-
cate that the early/middle Badenian boundary lies at 1374.5 m.
Within the early Badenian, at 1470 – 1490 m, the characteris-
tic Orbulina bloom was recorded (App. 1o). A rich foraminiferal
fauna with O. suturalis (down to 1590 m) and P. circularis, P.
glomerosa, U. macrocarinata and Cylindroclavulina rudis (down
to 1673 m) was observed. As in many drill cores, a less abun-
dant fauna occurs deeper down (1673 – 1867m). This part is
followed by a strong increase in agglutinated foraminifera,
comparable to the section in Perbersdorf 1. Scarce P. circula-
ris and P. glomerosa indicate Badenian sedimentation down
to 2127 m. In the well-log, the Karpatian/Badenian boundary
____
4.5 Petersdorf 1 deep well
strongly between the wells and subbasins. The distinct Styri-
an Unconformity separates the Karpatian and Badenian in the
Petersdorf 1 and Übersbach 1 wells, whilst continuous sedi-
mentation was recognized at Perbersdorf 1. At Übersbach1,
in the Fürstenfeld Subbasin, Badenian sedimentation started
with a basal conglomerate, whereas the other wells show si-
milar continuous deep-water conditions from the Karpatian to
the Badenian. Schreilechner and Sachsenhofer (2007) pre-
sented a sequence-stratigraphic interpretation based on seis-
mic sections of this area._____________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
Figure 13: Correlation of the investigated sections Katzengraben near Spi elfe ld, Wagna/old
brickyard and Retznei/main quarry, crossing the Karpatian/Badenian boundary._________________
5. Magnetostratigraphy
Stingl and Scholger (2005) check-
ed the palaeomagnetic measure-
ments of Auer (1996) in the Wagna
quarry, leading to minor corrections,
especially in the better-studied sec-
tion 3 that contains the Karpatian/
Badenian boundary. These re-inves-
tigations resulted in a sequence of
normal and reverse magnetic polari-
ties that could be assigned to dis-
tinct chrons using the established
biostratigraphic markers (Fig. 10).
Based on the Karpatian microfauna,
the normal polarity of the basal part
of section 3 must be assigned to
chron C5Cn.3n and the overlying re-
versal to chron C5Cn.2r. The marker
species Praeorbulina sicana in sam-
ple Wa 02/09 determines the polari-
ty chron in these beds as C5Cn.1n,
followed by the reverse chron C5Br.
By assigning the normal–reverse–nor-
mal polarity sequence in the coralli-
nacean limestones topping the sec-
tion with polarity chrons C5Bn.1n,
C5ADr and C5ADn, respectively, the
overlying beds, characterized by rhyth-
mically stratified brownish silty sand-
stones and siltstone layers, must be-
long to polarity chron C5Bn.1n (Fig.
10).
The results of palaeomagnetic mea-
surements in the Hauptstock and
Rosenberg sections in the Retznei
quarry (Stingl and Scholger 2005)
are shown in Fig. 11. In comparison
with the lithology and biostratigraphy
of the Wagna section (Geröllmergel),
both the normal polarity in the Karpa-
tian marls beneath the coral limesto-
ne must be placed in chron C5Cn.3n
and the single measurement in the
following coral limestone must be
__________________________
is shown by dipmeter measurement to be an angular uncon-
formity. The Karpatian sequence (2127 – 2342 m) contains a
scarce foraminiferal fauna with G. bisphericus and G. trilobus.
Uvigerinas are missing.
A correlation profile of the investigated wells, including the
published sections of Übersbach 1 and Fürstenfeld Th 1 is
shown in Fig. 9. Sedimentation started in most regions with a
thick cover of continental and limno-fluviatile clastics (Ottnan-
gian). The thickness of the marine Karpatian deposits varies
_______________________________
4.6 Correlation between wells
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
placed in chron C5Bn.1n (Figs 11, 12). The main section in the
Hauptstock, with a silt-clay sequence above corallinacean lime-
stones, shows normal polarity, interrupted by a few reversals
(Fig. 11). Since this section in part biostra-tigraphically belongs
to nannoplankton zone NN5 (Helicosphaera waltrans without
H. ampliaperta), it must be placed in chron C5ADn. This is ad-
ditionally shown by the radiometric dating of the tuffite layers.
40 39
Ar/ Ar dating of biotite and sanidine from the tuffite layer
on top of the corallinacean limestone in the Retznei main
quarry gave ages of 14.206 +/- 0.066 Ma and 14.39 +/- 0.12
Ma respectively (Handler et al. 2005, 2006). In the corallina-
cean limestone below and in the silty marls above the co-
occurrence of P. circularis and O. suturalis is observed. The
tuffite was deposited in the normal polarity chron C5ADn
(14.194 – 14.581 Ma). The marls above the tuffite encompass
all the investigated section at Retznei within the H. waltrans
horizon of Zone NN5 (Fig. 7). The LCO of H. waltrans, dated
at 14.357 Ma (Abdul Aziz et al., 2008) would support this. With-
in the upper part of the marls (samples R 02/07 – R 02/23), a
distinct increase in the occurrence of Paragloborotalia siaken-
sis left coiled is observed, which correlates with the upper part
of the acme abundance of this taxon in the Mediterranean
(DSDP – Site 372, Balearic Island) during chron C5ADn (up-
per part; Fig.12). This correlation indicates, together with the
H. waltrans horizon, that the sanidine age of 14.39 +/- 0.12
Ma from the Retznei main quarry is reliable.
Another radiometric age was determined on tuffites in a sec-
tion near Pöls, where shallow marine deposits of the Florian
Formation, rich in Lower Badenian mollusc faunas are present
(Kopetzky, 1957; Fritz et al., 2003). The foraminiferal fauna
consists of miliolids, Ammonia, Buccella, Nonion, Elphidium,
Cibicidoides and Amphistegina bohdanowiczi. Planktonic fora-
minifera are absent. The rare occurrence of H. ampliaperta
40 39
indicates nannoplankton Zone NN4. Ar/ Ar age dating of
sanidine crystals gave a plateau age of 15.75 +/- 0.17 Ma
(Handler et al. 2005, 2006). This age correlates the Florian
Formation with the earliest Badenian transgression in the Sty-
rian Basin during NN4 (chron C5Br, 15.160 – 15.974 Ma).
By comparisons with the Mediterranean stratigraphy, the bio-
stratigraphic and palaeomagnetic results have allowed the
time ranges of sedimentation gaps to be calculated between
the transgressions in the investigated near-shore localities
(Figs 10, 12, 13). In the basinwards positioned Wagna clay pit,
the time gap between polarity chrones C5Cn.2r and C5Cn.1n,
which contains the first Badenian transgression, was ca. 400 ky.
The second gap, between C5Br and C5Bn.1n, which includes
the second Badenian transgression and the NN4/NN5 boun-
dary, was ca. 600 ky (Figs 10, 12). This gap is much longer at
the near-shore Retznei quarry, where polarity chron C5Bn.1n
(NN5) directly follows C5Cn.3n (NN4), thus marking a time
gap of ca. 1.6 Ma (Figs 11, 13).
_
______________
___
________________________
6. Radiometric Dating and Biostratigraphy
7. Discussion
The correlation of calcareous nannoplankton and planktonic
foraminiferal events between the Styrian Basin and the Medi-
terranean demonstrates similarities caused by marine connec-
tions. In the case of benthic foraminifera, the marker species
for regional stratigraphy have been evaluated. Major bio-events,
such as some of the observed hiatuses and transgressions,
especially in near-shore areas, enables a correlation with the
rd
3 order sequences of Haq et al. (1988) and Hardenbol et al.
(1998). Similar results have been obtained by the interpreta-
tion of seismic lines in the eastern part of the basin (Schrei-
lechner and Sachsenhofer 2007).
To compare the global sequences with those of the Styrian
Basin, it was necessary to calibrate the curves with the new
time-scale and palaeomagnetic geochronology of Lourens et
al. (2004 a, b). The palaeomagnetic data of the Haq and Har-
denbol tables has been evaluated and correlated accordingly
(Tab. 3). The Karpatian transgression has been compared with
sequence TB 2.2, where the regression due to the falling-
stage system tract was intensified by tectonic movements of
the Styrian Tectonic Phase, forming angular unconformities
and leading to extreme shallowing and erosion. This was fol-
lowed by the first Badenian transgression of cycle TB 2.3 (Fig.
14) seen in the Wagna section between samples Wag02/08
and Wag02/19 as shallow water sediments with coral patch-
es (Fig. 10). The global sequence boundary Lan2/Ser1 was
found in the Wagna section above sample Wag02/19, follo-
wed by the transgressive cycle TB 2.4 of the far-spread Bade-
nian transgression that covered the entire Central Paratethys.
Although radiometric and biostratigraphical data indicate that
the youngest part of the investigated outcrops in Retznei be-
longs to the falling-stage system tract, the constantly increa-
sing water depth, seen in the benthic and planktonic foramini-
fera, demands tectonic subsidence. The sequence boundary
Ser2, compared with the Langhian/Serravallian boundary, was
only detected in the Petersdorf deep well 1.
_______________________
_______________
Table 3: Calibration of sequences. Based on the position in pa-
rd
laeomagnetic polarity chrons, global sequences of 3 order in Haq et
al. (1988) and Hardenbol et al. (1998) have been calibrated to the new
chron ages of Lourens et al. (2004a).__________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
Figure 14: Integrated stratigraphy of the Early/Middle Miocene with a revised cyclostratigraphic model for the Austrian Neogene basins. The dis-
continuous sections of the Wagna and Retznei outcrops, and the transition in the deeper parts of the Styrian Basin are shown. The additional sequen-
ce boundary at 14.20 Ma and cycle BA2/VB6 are given according to Kovač et al. (2004) and Strauss et al. (2006) based on seismic profiles in the Vi-
enna Basin.
8. Conclusion
At the early/middle Miocene boundary, that is, the Karpatian/
Badenian and Burdigalian/Langhian boundary, a series of
transgressive events in the Styrian Basin were combined with
tectonic events of the classical Styrian Tectonic Phase. The
formation of the Styrian Basin started during the early Mio-
cene, as swamp and floodplain deposits of probable Ottnan-
gian age, lying on top of the deeply eroded Austroalpine nap-
pes, were transgressed during the Karpatian by the Paratethys
Sea. A series of marine ingressions of the Badenian Sea fol-
lowed the deep water sediments of the Karpatian Steirischer
Schlier. During the Badenian, tectonic activity was accompa-
nied by extensive volcanism.
Changes in sedimentary facies and sedimentation rates, un-
conformities, sedimentation gaps, as well as tectonic and
volcanic activity demonstrate that the Styrian Phase was an
event that occurred around the early/middle Miocene boun-
dary. New stratigraphic results, in combination with palaeo-
magnetic and micropalaeontological investigations, allow the
timing of these events to be constrained. A major event is re-
presented in nearshore sediments between the sedimentation
of the Karpatian Steirischer Schlier and the lowermost Bade-
nian silts, with tilting of the Steirischer Schlier, to form the Sty-
rian Unconformity. The first Badenian transgression is repre-
sented in the Wagna section after a sedimentation gap be-
tween 16.5 and 16.1/16.2 Ma, while in deep wells of the cen-
tral basin sedimentation was continuous.
__________________________
_________________
The next sedimentation gap in nearshore regions occurred
around the nannoplankton zone NN4/NN5 boundary (14.74
Ma), between polarity chrons C5Br and C5Bn.1n, ranging
from about 15.4 to <14.8 Ma; this marks the second Badeni-
an transgression.
A third discontinuity, at the base of the corallinacean lime-
stones lying on top of the Wagna section, is too short to be
precisely dated. In the Retznei sections, this sedimentation
gap extends from top of the Karpatian Steirischer Schlier to
the base of the carbonate sedimentation, thus showing a large
gap between nannozones NN4 and NN5. At a few places,
sandy-silty sediments of the early Badenian are intercalated
below the carbonates of the Weissenegg Formation.
Volcanic ash layers and tuffites were deposited at the base
of marls and silts belonging to zone NN5 that overlie the coral-
linacean limestones of the Weissenegg Formation. The over-
lapping range of Praeorbulina and Orbulina, both present in
this upper section part, allows the assignment to chron C5ADn
(14.19 – 14.58 Ma), which is confirmed by radiometric dating.
rd
Although the global 3 order sequence marks a regression for
this period, the observed deepening tendency must have been
caused by continuing tectonic processes.
Investigations were performed within FWF projects P13743-
BIO, P16793-B06 and P13738-Tec of the Austrian Science
Fund. Field work was done in 2000, when the lower part of
____________________________________
_______
_________________
Acknowledgements
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
the Wagna section was investigated and in 2001 and 2002,
when the upper part of the Wagna section and the complete
Retznei section were investigated in detail, with support from
participants on a field course run by the Department of Pala-
eontology, University of Vienna. The Katzengraben section
was investigated during a field course in 2007. We especially
thank Silvia Spezzaferri (University of Fribourg, Switzerland)
for her work within project P13743-BIO. For support the samp-
ling work, we thank the owners of the old Wagna quarry and
of the Lafarge-Perlmooser Zement AG Retznei. We thank the
Rohöl-Aufsuchungs AG (Vienna) and the Austrian Geological
Survey for permission to study samples from deep wells. For
additional information on the region, we are grateful to our col-
leagues F. Ebner (Leoben), G. Friebe (Dornbirn), R. Handler
(Salzburg) and H. Hiden (Graz).________________________
_____________________________
____________________________
___________________
_
____________________
______________
_____________
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University of Vienna, Department of Palaeontology, Althanstrasse 14,
A 1090 Wien, Austria.
Natural History Museum Vienna, Burgring 7, A 1010 Wien, Austria.
Austrian Geological Survey, Neulinggasse 38, A 1030 Wien, Austria.
Istituto Ambiente Marino Costiero – CNR, Calata Porta di Massa, in-
terno Porto di Napoli, I-80133 Napoli, Italia.
University of Leoben, Department of Geosciences and Geophysics,
A 8700 Leoben, Austria.
Corresponding author, johann.hohenegger@univie.ac.at
______________________________________
__
_
____________________
____________________________________
__________
Received: 14. February 2009
Accepted: 12. May 2009
1)*) 2) 3)
Johann HOHENEGGER , Fred RÖGL , Stjepan ĆORIĆ , Pe-
1) 4) 3)
ter PERVESLER , Fabrizio LIRER , Reinhard ROETZEL , Ro-
5) 5)
bert SCHOLGER & Karl STINGL ______________________
1)
2)
3)
4)
5)
*)
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Appendix:
Wagna
Section
1
Sample
s
Calcidiscus leptoporus
Coccolithus miopelagicus
C. pelagicus
Cyclicargolithus floridanus
Discoaster deflandrei
D. musicus
Helicosphaera ampliaperta
H. carteri
H. scissura
H. walbersdorfensis
Reticulofenestra haqii
R. minuta
R. pseudoumbilica
R. gelida
Sph. heteromorphus
Sph. moriformis
Syracosphaera pulchra
Triquetrorhabdulus millowii
Umbilicosphaera jafarii
Wag26 r c r r r r f r r r f r r r r r r
Wag25 r r c r f r r r r r r
Wag24 r r c r r r f r r r r r r r
Wag23 r c r r f r r r r r f r r
Wag22 r r c r r f r r r r f r r
Wag21 r c r f r r r r r r r
Wag20 r r c r r f r r r r r f r r
Wag19 r r c r r r f r f r r f r r r
Wag18 r r c r r f r r r r f r r
Wag17 r c r r f r r r r f r r
Wag16 r c r r f r r f r r f r r
Wag15 r r c r r f r r r r r f r r
Wag14 r c r r f r r f r r f r r
Wag13 r r c r f r r r f r r
Wag12 r r c r r f r r r r r r r r r
Wag11 r r c r r f r r r f r r r
Wag10 r r c r r f r r r r r f r r r
Wag09 r c r r f r r r r r r
Wag08 r r c r r r f r r f r r f r r
Wag07 r r c r r r r r r r f r r r
Wag06 r c r r f r r r r r r r r
Wag05 r r c r r r f r r r r r r r r r r
Wag04 r r c r f r r r r r r r r r
Wag03 r r c r r f r r f r r r r r r
Wag02 r r c r r f r r f r r r r r
Wag01 r r c r r f r r f r r r r r
B A D E N I A N N N 4 (Martini, 1971) Stage/Nannoplankton Zone
Appendix 1A: Wagna brickyard; distribution of stratigraphically
important calcareous nannoplankton and biostratigraphic zonation in
section 1. a = abun dant , > 90% ; c = common, 50% – 90%; f = few,
10% – 50%; r = rare, < 10% of total abundance._________________
Nannoplankton Zones (Martini, 1971)
Wagna
Section 2
Samples
Calcidiscus leptoporus
Calcidiscus tropicus
C. miopelagicus
C. pelagicus
Cyclicargolithus floridanus
D. adamanteus
D. deflandrei
D. exilis
D. variabilis
H. ampliaperta
H. carteri
H. scissura
H. walbersdorfensis
Pontosphaera multipora
R. haqii
R. minuta
R. pseudoumbilica
R. gelida
S. heteromorphus
S. moriformis
Triquetrorhabdulus millowii
U. jafarii
Wag01/24 r r r c r r f r r r f r r r r r r
Wag01/23 r r c r r f r r r f r r r r r
Wag01/22 r r c r r f r r r r r r r r
Wag01/21 r c r r f r r f r r r r r
Wag01/20 r r r c r r r f r r r r r r r r r r
Wag01/19 r r r c r r r f r r r f r r r r r
Wag01/18 r r r c r r f r r r f r r r r r
Wag01/17 r c r r r f r r r f r r r r r
Wag01/16 r r r c r r r r r r r r r
Wag01/15 r r r c r r f r r r r r r r
Wag01/14 r c r r r r r r r r r r r
Wag01/13 r r c r r r r r r r r r
Wag01/12 r r r c r r r r r r r r r r
Wag01/11 r r r c r r r r r r r r r
Wag01/10 r r c r r r r r r r r r
Wag01/09 r r r c r r r r r r r r r
Wag01/08 r r c r f r r r r r r r
Wag01/07 r r r c r f r r r r r r
Wag01/06 r r c r r f 1 r r r r r r r
Wag01/05 r r r c r f 1 r r r r r r
Wag01/04 r r c r f r r r f r r r
Wag01/03 r r r c r f r r r r r f r
Wag01/02 r r r c r f r r f r r f r
Wag01/01 r r c r r r r r f r
K A R P T I A N B A D E N I A N
N N 4
Stage
Appendix 1B: Wagna brickyard; distribution of stratigraphically important calcareous nan-
noplankton and biostratigraphic zonation in section 2. a = abundant, > 90% ; c = common, 50% –
90%; f = few, 10% – 50%; r = rare, < 10% of total abundance.____________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
Wagna
Section 3
Samples
Stage
N (annoplankton Zones Martini, 1971)
Meters
Calcidiscus leptoporus
Coccolithus miopelagicus
Coccolithus pelagicus
Cyclicargolithus floridanus
Discoaster adamanteus
Discoaster deflandrei
Discoaster exilis
Discoaster variabilis
Helicosphaera ampliaperta
Helicosphaera carteri
Helicosphaera scissura
Helicosphaera walbersdorfensis
Helicosphaera waltrans
Reticulofenestra haqii
Reticulofenestra minuta
Reticulofenestra pseudoumbilica
Reticulofenestra gelida
Sphenolithus heteromorphus
Sphenolithus moriformis
Syracosphaera pulchra
Triquetrorhabdulus millowii
Umbilicosphaera jafarii
Wag02/25 0.3 r r f r f r r f c r r f r r
Wag02/24 2.3 r f r r f r r c r r f r r r
Wag02/23 5.9 r f r f r r c r r r r r
Wag02/22 7.3 r f f r f c r r r
Wag02/21 9.7 r r r r r r r a r
Wag02/20 10 r r r a r r r r
Wag02/19 11 r r c r f r f r r r r r r r
Wag02/18 12 r c r r r f r r f r r r r r r
Wag02/17 14 r c r r f r r r f r r r r r r
Wag02/16 15 r r c r f r r f r r r r r r
Wag02/15 17 r r c r r f r r r f r r r r r r
Wag02/14 18 f c r r f r r r f r r r r r
Wag02/13 18 r r c r f r r f r r r r r r r
Wag02/12 18 r c r r r f r r f r r r r r r r
Wag02/11 19 r c r r f r r r f r r r r r r
Wag02/10 19 r r c r r f r r r f r r r r r r
Wag02/9 19 r c r r f r r r f r r r r r r
Wag02/8 20 r c r r f r r r f r r f r r r r
Wag02/7 20 1 r c r f r f r r f r r
Wag02/6 21 r r c r r f r f r r r r r r
Wag02/5 22 r c r r r r r r r r r
Wag02/4 23 r r c r r r r r r r r r r r r
Wag02/3 24 r r c r r r r r r r r r r
Wag02/2 25 r c r f r r r r f r r
Wag02/1 25 r r c r f r r r r r f r r r r
NN4 NN5
KARPATIAN BADENIAN
Appendix 1C: Wagna brickyard; distribution of stratigraphically im-
portant calcareous nannoplankton and biostratigraphic zonation in section
3. a = abundant, > 90% ; c = common, 50% – 90%; f = few, 10% – 50%;
r = rare, < 10% of total abundance._______________________________
WAGNA
OLD
BRICKYARD
section 2
STAGES
WA 01/24 x x x
WA 01/23 x x x
WA 01/22 x x x
WA 01/21 x
WA 01/20 x x
WA 01/19 x x
WA 01/18 x x
WA 01/17 x x x
WA 01/16 x x x
WA 01/15 x x x
WA 01/14 x x x
WA 01/13 x x x
WA 01/12 x x
WA 01/11 x x
WA 01/10 x x
WA 01/9 x x
WA 01/8 x x x
WA 01/7 x x x
WA 01/6 x x
WA 01/5 x x x x
WA 01/4 x cf x x x
WA 01/3 x x x
WA 01/2 x x x
WA 01/1 x x x x
BADENIANKARPATIAN
small globigerinas
Globoturborotalita woodi
Globigerinoides bisphericus
Globigerinoides trilobus
Globigerinoides quadrilobatus
Praeorbulina circularis
Uvigerina graciliformis
Uvigerina laviculata
Pappina primiformis
Pappina parkeri
Appendix 1D: Wagna brickyard, section
2 in the southern part of the outcrop; stratigra-
phically important planktonic and benthic fora-
miniferal species in the upper part of the Kar-
patian and in the lower Badenian.__________
WA 02/25
WAGNA
OLD
BRICKYARD
section 3
small globigerinas
Globigerinoides bisphericus
Globigerinoides trilobus
Globigerinoides quadrilobatus
Praeorbulina sicana
Praeorbulina transitoria
Praeorbulina glomerosa
Praeorbulina circularis
Orbulina suturalis
Uvigerina graciliformis
Pappina primiformis
Pseudogaudryina lapugyensis
Paragaudryinella interjuncta
Amphistegina mammilla
Remarks
STAGES
x x x x x x x x x x x
WA 02/24 x x x x x x x x
WA 02/23 x x x x x x x
WA 2002/3 x x x x x x
WA 02/22 x x x x x x x x x x
WA 2002/2 x x x x x x x x
WA 2002/1
WA 02/21 x x
WA 02/20 x x
WA 02/19 x x
WA 02/18 x x x
WA 02/17 x x x
WA 02/16 x x x
WA 02/15 x x x x
WA 02/14 x x
WA 02/13 x
WA 02/12 x x
WA 02/11 x x
WA 02/10 x x
WA 02/9 x x x
WA 02/8 x x
WA 02/7 x x x
WA 02/6 x x x
WA 02/5 x x x
WA 02/4 x x x
WA 02/3 x x x
WA 02/2 x x x
WA 02/1 x cf x x
BADENIANKARPATIAN
corallinacean
limestone with
volcanic mica
sandstone and
sand
patch reef
Appendix 1E: Wagna brickyard, section 3 in the nor-
thern part of the outcrop; important planktonic and benthic
foraminiferal species in the upper part of the Karpatian and
lower Badenian. The Styrian Unconformity and subdivision
of Badenian sediments is demonstrated.______________
Re 00/8
Retznei
Section 00
Samples Stage
Nannoplankton Zones (Martini, 1971)
Coccolithus miopelagicus
Coccolithus pelagicus
Coronocyclus nitescens
Cyclicargolithus floridanus
Helicosphaera ampliaperta
Helicosphaera carteri
H. waltrans
H. scissura
Reticulofenestra gelida
R. haqii
R. minuta
R. pseudoumbilica
Sphenolithus heteromorphus
Sph. moriformis
Syracosphaera pulchra
Triquetrorhabdulus milowii
Umbilicosphaera jafarii
Badenian NN5 f r r r a r r
Re 00/7 r c r r f r r r r r r r r
Re 00/6 c r r f r r r r r r r r
Re 00/5 c r r f r r r f r r r
Re 00/4 r c r r f r r f f r r r r
Re 00/3A r c r r r r r f r r r r r
Re 00/3 r c r r f r r r f r r r r
Re 00/2 r c r r r f r r f r r r r r
Re 00/1 r c r r r f r r r r r r r r
Karpatian
NN4
Appendix 1F: Retznei, Lafarge-Perlmooser Cement Factory, main quar-
ry, section in the center of the quarry (Friebe 1988, 1993). Stratigraphically im-
portant calcareous nannoplankton and biostratigraphic zonation. a = abundant,
> 90% ; c = common, 50% – 90%; f = few, 10% – 50%; r = rare, < 10% of to-
tal abundance.
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
R 01/38
Retznei
Section
01
Samples
Stage/Nannoplankton Zone
m
Coccolithus miopelagicus
C. pelagicus
Coronocyclus nitescens
Cyclicargolithus floridanus
Discoaster adamanteus
D. exilis
D. formosus
D. musicus
D. variabilis
Geminilithella rotula
Helicosphaera carteri
H. walbersdorfensis
H. waltrans
Reticulofenestra haqii
R. minuta
R. pseudoumbilica
R. gelida
Rh. sicca
S. heteromorphus
S. moriformis
Syracosphaera pulchra
Umblicosphaera jafarii
R 01/39 2 r r r r r r r r a r r r r r r
3 r r r r r r r r r r a r r r r r r
R 01/37 4 r r r r r r r r r r a r r r r r
R 01/36 5 r r r r r r r r a r r r r r
R 01/35 6 r r r r r r r a r r r r r r r
R 01/34 7 r r r r r r r r a r r r r r r
R 01/33 8 r r r r r r r a r r r r r r
R 01/32 9 r r r r r r c r r r r r r
R 01/31 10 f r r r r r c r r r r r
R 01/30 10.8 r f r r r r r c r r r r r r r
R 01/29 11.3 f r r r r r r c r r r r r r
R 01/28 12.2 r r r r a r r r r r r r
R 01/27 13.7 f r r r r r c r r r r r
R 01/26 14.7 f r r r r r c r r r r
R 01/25 15.7 r f r r r r c r r r r r
R 01/24 16.7 f r f r r r c r r r r r
R 01/23 17.7 f r r r c r r r r r r
R 01/21 19 f r r r r c r r r r r r
R 01/20 20.1 f r r f c r r r r r
R 01/19 20.8 f r r r r c r r r r r r r
R 01/18 21.5 r f r r r f c r r r r r
R 01/17 22.1 f r r r r f c r r r r r r
R 01/16 22.5 f r r r r r r c r r r r r r
R 01/15 23.6 c r r r
R 01/14 24.7 f r r r r r r r r a r r r r r
R 01/13 25.2 f/c r r r r r r r c r r r r r
R 01/12 25.6 f r r r r r r r c r r r r r r
R 01/11 26.7 f r r r r r c r r r r r
R 01/10 27.7 f r r r r r c r r r r r
R 01/9 28.5 f r r r r c r r r r r
R 01/8 29.2 f r r
R 01/7 29.8 f r r r c r r r r r
R 01/6 30.2 f r r r r c r f r r r
R 01/5 30.6 f r r r c r r r r
R 01/4 31.6 r f r r r r r r c r r r r r
R 01/3 33.4 f r r r r r c r r r r r r
R 01/2 33.7 f r r r c r r r r r r
R 01/1 35 r 69 r r r r r c r r r r r r
B A D E N I A N N N 5 (Martini, 1971)
Appendix 1G: Retznei, Lafarge-Perlmooser Cement Factory, main
quarry, section R 01. Stratigraphically important calcareous nannoplankton
and biostratigraphic zonation. a = abundant, > 90% ; c = common, 50% –
90%; f = few, 10% – 50%; r = rare, < 10% of total abundance.__________
R 02/33
Retznei
Section 02
Samples
Coccolithus miopelagicus
C. pelagicus
Coronocyclus nitescens
Cyclicargolithus floridanus
Discoaster adamanteus
D. exilis
D. formosus
D. musicus
D. variabilis
Discoaster sp.
Geminilithella rotula
Helicosphaera carteri
H. walbersdorfensis
H. waltrans
Pontosphaera multipora
Reticulofenestra haqii
R. minuta
R. pseudoumbilica
R. gelida
Rhabdosphaera sicca
Sphenolithus heteromorphus
S. moriformis
Syracosphaera pulchra
Thoracosphaera spp.
Umblicosphaera jafarii
barren
R 02/32 barren
R 02/31 r r r r f c r r
R 02/30 r c r r r r r f f r r r r r
R 02/29 f r r r r f c r r r r
R 02/28 f r r f c r r r
R 02/27 f r f c r r r
R 02/26 r f r r f c r r
R 02/25 r f/c r r r r r r f/c r r r
R 02/24 r f r r r r f r r r r r
R 02/23 f r r r r c r r
R 02/22 f r r c r r r r
R 02/21 r r r f c r r r
R 02/20 r r r r f c r r r r
R 02/19 r r r r c r r r r r
R 02/18 f r r r r r r r r r c r r r r r r r r
R 02/17 r r r c r r
R 02/16 r r r r r f c r
R 02/15 f r r f c r r r
R 02/14 f r r c r r r r r
R 02/13 r r r r r r r f c r r r r r
R 02/12 f r r r r c r r r r r r
R 02/11 r r r r r r c r
R 02/10 f r r r r c r
R 02/9 r r r r r f c r r r
R 02/8 r r r r r c r r r r r r
R 02/7 f r r r r r r r c r r r r r
R 02/6 r r r c r r
R 02/5 r r r r r c r r r r r
R 02/4 f r r r r r c r r r r
R 02/3 r r r r r r r r r r r c r r r r
R 02/2 f r r r r r r c r r
R 02/1 r f r r r r r r r r c r r
B A D E N I A N N N 5 (Martini, 1971) Stage/Nannoplankton Zone
Appendix 1H: Retznei, Lafarge-Perlmooser Cement Factory, main quarry, section
R 02. Stratigraphically important calcareous nannoplankton and biostratigraphic zonation.
a = abundant, > 90% ; c = common, 50% – 90%; f = few, 10% – 50%; r = rare, < 10% of
total abundance.___________________________________________________________
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
RETZNEI - MAIN QUARRY
sample number
R 02/32
R 02/31
R 02/30
R 02/29
R 02/28
R 02/26
R 02/22
R 02/20
R 02/15
R 02/10
R 02/05
R 02/04
R 01/25
R 01/24
R 01/21
R 01/20
R 01/15
R 01/10
R 01/07
R 01/02
"Geröll-
mergel"
RE2002-2
Karpatian
RE2002-1
Marginulina hirsuta
Melonis pompilioides
Myllostomella advena
Myllostomella recta
x x x
x
x x
x x x x
x x x
x x x x
x x x x
x x x
x x x
x x
x x x
x x x
x x x
x x x
x x
x x
x x
x x x x
x x
x x
x x x
x x x x x x x x x x x x x x x x x x
x x x
x x x x x x x x x x x
x x x x x x x x x x x x x
x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x x x x x x x
Bolivina antiqua
Bolivina cf. lowmani
Bolivina dilatata
Bolivina fastigia
Bolivina hebes
Bolivina plicatella
Bolivina pseudoplicata
Bolivina scalprata retiformis
Bulimina buchiana/striata
Cancris auriculus
Caucasina subulata/schischkinskayae
Charltonina tangentialis
Chilostomella ovoidea
Chrysalogonium longicostatum
Cibicidinella ? sp. (wuellerstorfi)
Cibicidoides austriacus/variolatus
Cibicidoides pachy derma/ spp.
Cibicidoides ungerianus
Conorbella paradoxica
Coryphostoma digitalis
Dentalinaspp.
Dyocibicides biserialis
Ehrenberginaserrata
Elphidiella subnodosa/minuta
Elphidium spp.
Eponides repandus
Fursenkoina acuta
Gavelinopsis praegeri
Glandulina laevigata
Glandulopleurost. pleurostomelloides
Globobulimina pupoides/pyrula
Globocassidulina cruysi
Globocassidulina oblonga
Globocassidulina subglobosa
Globulina gibba/punctata
Grigelis pyrula
Guttulina communis/austriaca
x x x x x x x x
x x x x x x x x x
Guttulina irregularis
Gyroidinoides soldanii/umbonatus
Hanzawaia boueana
Hemirobulina spp.
Heterolepa dutemplei/praecincta
Laevidentalina spp.
Lamellodiscorbis cf. dimidiatus
Lapugyina schmidi
Lenticulina spp.
Lingulina costata
Lobatula lobatula
x
x x x x x x x
x x x
x x x x x
x x x x x
x x x x x
x x x x x x x x
x x x x x x x
x x x x x x x x
x x x x x x x
x x x x x
x x x x x x x x
x x x x x x x
x x x x x x x
x x x x x x x
x x x x x x x x
x x
x x x x x x x x
x x x x x x x
x x x x x x x x
x x x x x x x x
x x xx
Appendix 1I continue
Appendix 1I: Retznei, Lafarge-Perlmooser Cement Factory, main quarry, sections R 01 – R 02. Distribution of benthic foraminiferal species in
the Badenian sediments. The isolated outcrop with Karpatian Steirischer Schlier (RE 2002-1) and Geröllmergel (RE 2002-2) is shown at the base of
the table.
RETZNEI - MAIN QUARRY
sample number
R 02/32
R 02/31
R 02/30
R 02/29
R 02/28
R 02/26
R 02/22
R 02/20
R 02/15
R 02/10
R 02/05
R 02/04
R 01/25
R 01/24
R 01/21
R 01/20
R 01/15
R 01/10
R 01/07
R 01/02
"Geröll-
mergel"
RE2002-2
Karpatian
RE2002-1
Alveolophragmium crassum
Ammodiscus miocenicus /spp.
Ammomarginulina? matchigarica
Bathysiphon filiformis
Bigenerina agglutinans
Bigenerina directa
Budashevaella laevigata/wilsoni
Cribrostomoides spp.
Cribrostomoides subglobusus
Cyclammina karpatica
Cylindroclavulina rudis
Gaudryinopsis beregoviensis
Gaudryinopsis megagranosus
Glomospira charoides
Haplophragmoides spp.
Hyperammina elongata
Hyperammina granulosa
Karreriella badenensis
Karrerulina apicularis
Karrerulina horrida/conversa
Martinotiella communis
Martinotiella karreri/perparva
Paravulvulina serrata
Popovia sp.
Psammolingulina papillosa
Psammosphaera fusca
Pseudogaudryina lapugyensis
Pseudogaudryina mayeriana
Pseudogaudryina sturi
Reophax brevior/scorpiurus
Reticulophragmium karpaticum
Reticulophragmium obliquicameratu m
Reticulophragmium venezuelanum
Rhabdammina sp.
Rhizammina sp.
Semivulvulina deperdita/pectina ta
Siphotextularia flexua/concav a
Spirorutilus carinatus
Textularia gramen
Textularia laevigata
Textularia lanceolata
Textularia mariae
Tritaxis rara
Vulvulina cf. pennatula
x x
x x x
x x x
x x x x
x x x
x x x x x
x
x x x
x x
x x
x x
x x
x x
x x x
x x x
x
x x x
x x x x
Ammonia spp.
Amphicoryna spp.
Amphimorphina haueriana
Amphistegina bohdan./mamm illa
Angulogerina angulosa
Anomalinoides badenensis
x x x
x x x
x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x
x x
x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x x x x
x x x x
x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x c x x x x
x x x x x x x x x x x x x x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x x
x
x x x x x x x x x x x x
x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x x x x
x x x x x x x x
x x x x x
x
x
x
x
Asterigerinata mamilla/planorbis
Baggina arenaria
x
x
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Appendix 1I continue
RETZNEI - MAIN QUARRY
sample number
R 02/32
R 02/31
R 02/30
R 02/29
R 02/28
R 02/26
R 02/22
R 02/20
R 02/15
R 02/10
R 02/05
R 02/04
R 01/25
R 01/24
R 01/21
R 01/20
R 01/15
R 01/10
R 01/07
R 01/02
"Geröll-
mergel"
RE2002-2
Karpatian
RE2002-1
Uvigerina pygmoides
Uvigerina semiornata
Uvigerina uniseriata
Vaginulina legumen
Vaginulinopsis spp.
Valvulineria complanata
x x
x x
x x x
x x
x x x
x x x x x
x x x x x
x
x x
x x x
x x
x x x x
x x x
x x x x
x
x x x
x x
x x x
x
x
Neoeponides schreibersi
Neolenticulina peregrina
Neugeborina longiscata/irregularis
Nodosarella rotundata/ sp.
Nodosaria guttifera
Nonion commune
Nonionella turgida
Nonionoides ventragranosus
Oridorsalis umbonatus
Orthomorphina spp.
Pandaglandulina elliptica/ sp.
Pappina parkeri
Pappina primiformis/breviformis
Pararotalia aculeata
Planularia dentata/cassis
Planularia lanceolata
Plectofrondicularia spp.
Pleurostomella alte rnans/ spp.
Porosononion granosum
Pseudonodosaria brevis/ sp.
Pseudoparrella exigua
Pullenia bulloides/quinqueloba
Pyramidulina raphanistrum
Pyramidulina spp.
Pyrgo simplex/lunula
Quinqueloculina/Cycloforina spp.
Riminopsis boueanus
Rosalina globularis
Sigmoilinita tenuis
Sigmoilinita tschokrakensis
x x
x x x x x x x x x
x
x x x x x x x x
x x x x x x x x x x
x x x x x x x x x
x x x x x x x x x x
x x x x x x x x x x
x x x x x x x x x x x x x x x x x x x
x x x x x x x
x x x x x x x x x x x
x x x x x x x x x x x x x
x x x x x x x x x x x x
x x x x x x x x x x x x
x x x x x x x x x x x x x x
x x x x x x x x x x x x x
x x x x x x x x x x x x x
x x x x x x x x x x x
x x x x x x x x x x x x x x x x
x x x x x x x x x x x
x x x xx x x
Sigmoilopsis foeda/celata
Siphogenerinoides vasarhelyi
Siphonina reticulata
Siphonodosaria adolphina
Siphonodosaria consobrina/verneuli
Siphonodosaria s cabra/scripta/ sp.
Sphaerogypsina globulus
Sphaeroidina bulloides
Spiroloculina excavata/canalic ulata
unilocular (Lagena, Fissurina etc.)
Uvigerina aff. barbatula
Uvigerina cf. bulbacea
Uvigerina graciliformis
Uvigerina grilli
Uvigerina laviculata
Uvigerina macrocarinata
x
x x x x x x x x x
x x
x x x x x
x x x x x
x x x x x x x
x x x x x x x x
x x x x x x x x
x x x x x x x x x x
x x x x x x
x x x x x
x x x x x x x x x x
x x x x x x x x
x x x x x x x x
x x x x x x x x x
x x x x x x x x x
x
x x x x x x x x x
x x x x x x x x
x x x x x x x x x
x x x x x x
x
RETZNEI - MAIN QUARRY
sample number
Cassigerinella globulosa
Globigerina bollii
Globigerina bulloides
Globigerina concinna
Globigerina diplostoma
Globigerina falconensis
Globigerina ottnangiensis
Globigerina praebullodies
Globigerina subcretacea
Globigerina tarchanensis
Globigerinella regularis/opinata
Globigerinita glutinata
Globigerinita uvula
Globigerinoides apertasuturalis
Globigerinoides bisphericus
Globigerinoides quadrilobatus
Globigerinoides trilobus
Globoquadrina cf. altispira
Globorotalia bykovae
Globorotalia peripheroronda
Globorotalia praescitula
Globorotalia transsylvanica
Globoturborotalita druryi
Globoturborotalita woodi
Orbulina suturalis
Paragloborotalia inaequiconica
Paragloborotalia siakensis/acrostoma
Praeorbulina cf. sicana
Praeorbulina circularis
Praeorbulina glomerosa/curva
Tenuitella clemenciae
Tenuitella minutissima
Tenuitellinata angustiumbilicata
Tenuitellinata selleyi
Turborotalita neominutissima
Turborotalita quinqueloba
Bachmayerella tenuis
Bachmayerella sp.
Bolboforma moravica
Bolboforma reticulata
black volcanic mica
sanidine
Remarks
R 02/32 x x x x x x x x x x x xstrongly corroded/pyrityzed
R 02/31 x x x x x x x x x x x x x x x x x x x x x Orbulina horizon
R 02/30 x x x x x x x x x x x x x x gypsum
R 02/29 x x x x x x x x x x x x x x x x x x x x x x x Globigerina horizon
R 02/28 x x x x x x x x x x x x x x x x x x x x
R 02/26 x x x x x x x x x x x x x x x x x x x x x x x Globigerina horizon
R 02/22 x x x x x x x x x x x x x x x x x x x x G. bykovae horizon
R 02/20 x x x x x x x x x x x x x x x x x x x
R 02/15 x x x x x x x x x x x x x x x x x x x x x
R 02/10 x x x x x x x x x x x x x x x x x x
R 02/05 x x x x x x x x x x x x x x x x
R 02/04 x x x x x x x x x x x x x x x x x x
R 01/25 x x x x x x x x x x x x x x x x x x x x x x x x x x x
R 01/24 x x x x x x x x x x x x x x x x
R 01/21 x x x x x x x x x x x x x x x
R 01/20 x x x x x x x x x x x x x
R 01/15 x x x x x x x x x x x x x smektite? with pumice
R 01/10 x x x x x x x x x x Globigerinoides horizon
R 01/07 x x x x x xamount of glauconite
R 01/02 x x x x x x x x x x x x x x x x x x corallinacean marl
"Geröllmergel"
RE2002-2 x x x x x x x silt with pebbles
Karpat
RE2002-1 x x x x x cf cf x cf x dark calcareous shale
Orbulina horizon
Globigerinoides horizon
Appendix 1J: Retznei, Lafarge-Perlmooser Cement Factory, main quarry, sections R 01 – R 02. Distribution of planktonic foraminiferal species
in the Badenian sediments. The isolated outcrop with Karpatian Steirischer Schlier (RE 2002-1) and Geröllmergel (RE 2002-2) is shown at the base of
the table.
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
KARPATIAN
Katzengraben
section
Stage
Nannoplankton Zones (Martini, 1971)
Braarudosphaera bigelowii
Calcidiscus leptoprorus
Cd. premacintyrei
Cd. tropicus
Coccolithus miopelagicus
C. pelagicus
Coronosphaera mediterranea
Cyclicargolithus floridanus
Discoaster deflandrei
D. variabilis
Helicosphaera ampliaperta
H. carteri
H. euphratis
H. granulata
H. scissura
H. walbersdorfensis
H. waltrans
Pontosphaera multipora
Reticulofenestra gelida
R. haqii
R. minuta
R. pseudoumbilica
Sphenolithus heteromorphus
S. milanetti
S. moriformis
Umbilicosphaera jafarii
C2/1 r f r r f r r r r c r r
C2/01 r r f r r r r r r r c r r
C1/01 r c r r f r r r r
B04 f r r r f r r r f c r
B03 r r r f r r r r r r r f c r
B02 r c r r r f r r r f r r r
B01 r c r r r r f r r r r r f r r r
A06 r r f r f r c r r r r f r r
A05 c r r f r r r
A04 r c r r r r f r r r r r r r r
A03 r c r r r r f r r r r r r f r r
A02 c r r f r r
A01 r c r f f r r r r f r
BADENIAN
N N 5N N 4
Appendix 1K: Katzengraben. Stratigraphically important calcareous nannoplankton and bio-
stratigraphic zonation. a = abundant, > 90% ; c = common, 50% – 90%; f = few, 10% – 50%; r = rare,
< 10% of total abundance.____________________________________________________________
PERBERSDORF 1 Stage
246.00-247.00 m r f f f f f a r f f
299.00-304.00 m f f r f f c f r f f
346.00-352.00 m f r f r r r a r r
364.00-370.00 m r r f r f r r f f c r f r r
382.00-388.00 m r f r f r f c r f r r
388.00-394.00 m f f f f c f f
461.00-467.00 m r r f f f r r f c r r
492.00-490.00 m r f r f r r r f f c f f f r r
496 m r c r r r r r r r r
520.00-523.00 m r r c f f f r r r r r r r f r r
527.40-534.00 m
557.00-563.00 m
628.20-632.20 m
661.1 m
689 m
689.00-694.00 m
729.00-732.50 m
746 m c r r
785.80-794.00 m r c r f r r r r
809.00-811.00 m r c r f r r r r r
850.00-856.00 m r r c f f r r f r r r r
868.00-874.00 m r c r f r r r f r
933.00-939.00 m r c r f r f r
947.5-1311m barren
B A D E N I A N
N N 4 N N 5
Volcanic level No nannofossils
KARPATIAN
Nannoplankton Zones (Martini, 1971)
Calcidiscus leptoporus
Coccolithus miopelagicus
Coccolithus pelagicus
Cyclicargolithus floridanus
Helicosphaera ampliaperta
Helicosphaera carteri
Helicosphaera scissura
Helicosphaera walbersdorfensis
Helicosphaera waltrans
Pontosphaera multipora
Reticulofenetra bisecta
Reticulofenestra gelida
Reticulofenestra haqii
Reticulofenestra minuta
Reticulofenestra pseudoumbilica
Rhabdosphaera sicca
Sphenolithus heteromorphus
Sphenolithus moriformis
Triquetrorhabdulus milowii
Umbilicosphaera jafarii
Appendix 1L: Perbersdorf deep well 1; distribution of stratigraphically important calcareous nan-
noplankton. a = abundant, > 90% ; c = common, 50% – 90%; f = few, 10% – 50%; r = rare, < 10% of
total abundance._____________________________________________________________________
Appendix 1M: Perbersdorf deep well 1; distri-
bution of important planktonic foraminifera.________
PERBERSDORF 1
Planktonic Foraminifera
Core Sample
box number
Sample Depth in Metres
216-223 3 220 x x x
246-247 246 x x x x x x x x x
247-248 247 x x x x x x x
252-258 255 x x x x x cf.
270-276 1 275 x x x x x x x x x x x
276-282 3 279 x x x x x x x x x x x
276-282 2 280 x x x x x x x x x
282-288 285 x x x x x x
288-293 291 x x x x x x
299-304 302 x x x x
304-310 307 x x x x x
310-316 2 314 x x x x x
310-316 1 315 x x x x
316-322 2 320 x x x
316-322 1 321 x x x x
328-334 3 331 x x x x x x
328-334 2 332 x x x x x
328-334 1 333 x x x
Orbulina suturalis
Praeorbulina glomerosa circularis
Globigerinoides trilobus
Globigerinoides quadrilobatus
Globigerinoides bisphericus
Globoquadrina cf. altispira
Globoquadrina cf. globosa
Globorotalia transsylvanica
Globorotalia peripheroronda
Praeorbulina transitoria
Paragloborotalia mayeri
Globorotalia bykovae
Praeorbulina sicana
Praeorbulina glomerosa glomerosa
ZONATION
Lagenidae Zone - NN5
1 804.2
805.2-809 807 x
809-811 810.5
838-844 841
844-850 847
850-856 853
856-862 859
862-868 865
868-874 871
874-880 877
880-886 883
800.9-805.2
Karpatian - NN4
886-896 891
902-908 905
914-920 917
924.7-930.8 927.8
933-939
959.5-965.5 1 965
976-982
982-988
988-994
994-1000
1000-1006 ? ? ?
1009-1015
1025.8-1032.0
1043.4-1049.2
1963-1068
1114.3-1120.3
1191-1193
1290.0-1295.7
1352-1354
1397.5-1403,5
Ottnangian - Karpatian
334-340 3 337 x x x x x xx
334-340 2 338 x x x x x x xx
334-340 1 339 x x x x x xx
346-352 349 x x x x x xx
352-358 2 356 x x
352-358 1 357 x x x x x x
358-364 361 x
364-370 367 x x x x x xx
370-376 373 x x xx
376-382 2 380
376-382 1 381
382-388 2 386
382-388 1 387
388-394 2 392 x
388-394 1 393 x
394-400 397
400-405.5 2 403.5
400-405.5 1 404.5
405.5-411.5 2 409.5
405.5-411.5 1 410.5
411.5-417 414
417-422 419
422-427.4 425 x x x cf.
427.4-432.8 2 430.8
427.4-432.8 1 431.8
432.8-438.5 435.5
438.5-444 2 442 cf.
438.5-444 1 443
444-450.5 2 448.5 x
444-450.5 1 449.5
450.5-456 2 454
450.5-456 1 455 x x
456-461 458.5 x
461-467 464
467-473 470
473-479 476
479-485 482 x
485-491 2 489
485-491 1 490
491-496.5 493.5
496.5-502.5 4 498.5
496.5-502.5 3 499.5
496.5-502.5 2 500.5
496.5-501.5 1 501.5
508.5-514 x x x
514-520 2 518
514-520 1 519
520-523 521.5
523-527.7 525.5
527.7-534.2 530.5
534.2-540 537
545-551 548
557-565 561
568-574 571
587-591 589 x x
606.5-612.7 609.5 x ?
620.2-626.2 623.2
666.1-669.3 667.6
675.4-676.8 675
689-694.8 692
718-721 719.5
721-727 724
746-749 747.5
749-752.4 2 750.4
749-752.4 1 751.4
752.4-758.8 755.6
764-769 766.5
780.1-783.4 781.6
783.4-786.7 785
786.7-794 790
796-800.9 798.5
800.9-805.2 2 803.2 x
Lagenidae Tone - NN4
PERBERSDORF 1
Planktonic Foraminifera
Core Sample
box number
Sample Depth in Metres
Orbulina suturalis
Praeorbulina glomerosa circularis
Globigerinoides trilobus
Globigerinoides quadrilobatus
Globigerinoides bisphericus
Globoquadrina cf. altispira
Globoquadrina cf. globosa
Globorotalia transsylvanica
Globorotalia peripheroronda
Praeorbulina transitoria
Paragloborotalia mayeri
Globorotalia bykovae
Praeorbulina sicana
Praeorbulina glomerosa glomerosa
ZONATION
Lagenidae Zone - NN5
Johann HOHENEGGER, Fred RÖGL, Stjepan ĆORIĆ, Peter PERVESLER, Fabrizio LIRER, Reinhard ROETZEL, Robert SCHOLGER & Karl STINGL
Appendix 1N: Perbersdorf deep well 1; distribution of important benthic
foraminifera and remarks on faunal events.____________________________
PERBERSDORF 1
Benthic Foraminifera
Core Sample
box number
Sample Depth in Metres
Remarks
216-223 3 220 x x x
246-247 246 x x x x x x x
247-248 247 x x x x x x Orbulina bloom
252-258 255 x x x x
270-276 1 275 x x x x x x
276-282 3 279 x x x x x
276-282 2 280 x x x x x x
282-288 285 x x cf. x x
288-293 291 x x x x x x x
299-304 302 x cf. x x x x
304-310 307 x x x
310-316 2 314 x cf. x x
310-316 1 315 x x x x x
316-322 2 320 x
316-322 1 321 x x x x x
328-334 3 331 x x x cf. x x
328-334 2 332 x cf. x x x
328-334 1 333
334-340 3 337 x x cf. x x x x x
334-340 2 338 cf. x x x
334-340 1 339 x x cf. x x
346-352 349 x cf. x x
352-358 2 356 poor assemblage
352-358 1 357 x x x cf. x x x
358-364 361 x poor assemblage
364-370 367 x x x
370-376 373 x x x x x
376-382 2 380 x x cf. x x x
376-382 1 381 x x cf. x x x x
382-388 2 386 x x x cf. x
382-388 1 387 x x x x x x
388-394 2 392 x x x x x x x
388-394 1 393 x x x
394-400 397 x x x x x
400-405.5 2 403.5 x cf. x x x
400-405.5 1 404.5 x x x x ?
405.5-411.5 2 409.5 x x
405.5-411.5 1 410.5 x x cf. x
411.5-417 414
417-422 419
422-427.4 425 cf. cf. cf.
427.4-432.8 2 430.8 x x
427.4-432.8 1 431.8 x cf. x poor assemblage
432.8-438.5 435.5 x
438.5-444 2 442 cf. x x
438.5-444 1 443 cf. x poor assemblage
444-450.5 2 448.5 x x cf. x x x
444-450.5 1 449.5 x x x x x x x x
450.5-456 2 454 x x
450.5-456 1 455 x x x x x
poor assemblage
456-461 458.5 x cf. x
461-467 464 cf. x x
467-473 470 x x cf. x x x x x
473-479 476 x
479-485 482 x
485-491 2 489 x
485-491 1 490 x x x
Uvigerina pygmoides
Uvigerina macrocarinata
Uvigerina uniseriata
Uvigerina cf. pudica
Uvigerina aculeata
Uvigerina cf. costai
Uvigerina semiornata
Uvigerina grilli
Uvigerina cf. bulbacea
Uvigerina acuminata
Uvigerina graciliformis
Uvigerina parviformis
Uvigerina cf. laviculata
Pappina primiformis
Uvigerina cf. barbatula
Uvigerina sp. (striate)
Vaginulina legumen
Colominella paalzowi
Cylindroclavulina rudis
Psammolingulina papillosa
Pseudogaudryina sturi
491-496.5 493.5
880-886 883 x x x
886-896 891 x x
902-908 905 x
496.5-502.5 4 498.5 x
496.5-502.5 3 499.5 x x
496.5-502.5 2 500.5 x
496.5-501.5 1 501.5 x
508.5-514 511 x x x
514-520 2 518 x
514-520 1 519 x
520-523 521.5 x x
523-527.7 525.5 poor assemblage
527.7-534.2 530.5 cf. x x xx x
534.2-540 537 x
545-551 548 x
557-565 561
568-574 571
587-591 589
606.5-612.7 609.5
620.2-626.2 623.2 Bathysiphon
assemblage
666.1-669.3 667.6 barren
675.4-676.8 675 x xx x x
689-694.8 692 x x
718-721 719.5
721-727 724
746-749 747.5 x x
749-752.4 2 750.4 cf. x
749-752.4 1 751.4 x x x
752.4-758.8 755.6 x x x x
764-769 766.5 x x
780.1-783.4 781.6 cf. x x
783.4-786.7 785 x x x x x
786.7-794 790 x x
796-800.9 798.5 x x
800.9-805.2 2 803.2 cf. x x x
800.9-805.2 1 804.2 cf. x x x x
805.2-809 807 cf. x x
809-811 810.5 x x
838-844 841 x x x x
844-850 847 x x x
850-856 853
856-862 859 x
862-868 865 x x
868-874 871 x
874-880 877 x x
Bathysiphon
assemblage
Bathysiphon
assemblage
poor assemblage
Appendix 1M continue
The Styrian Basin: a key to the Middle Miocene (Badenian/Langhian) Central Paratethys transgressions
PETERSDORF 1
cuttings/meter
Globigerinoides bisphericus
Globigerinoides trilobus
Praeorbulina glomerosa circularis
Orbulina suturalis
Globoquadrina cf. altispira
Globigerinoides quadrilobatus
Globorotalia bykovae
Globorotalia transsylvanica
Praeorbulina glomerosa glomerosa
Praeorbulina transitoria
Uvigerina semiornata
Uvigerina grilli
Uvigerina aculeata
Pappina parkeri
Uvigerina cf. bulbacea
Uvigerina pygmoides
Uvigerina acuminata
Uvigerina macrocarinata
Pappina primiformis
Lenticulina ariminensis
Lenticulina orbicularis
Lenticulina echinata
Pyramidulina raphanistrum
Paragaudryina interjuncta
Cylindroclavulina rudis
Pseudogaudryina lapugyensis
STRATIGRAPHY
1410 x x x x x x x
1430 x x x x x x x x x x x
1450 x x x x x x x x x x x
1470 x x x x x
1490 x x x x x x
1510 x x x x x x x x x x x x cf.
1530 x x x x x x x x x cf. x
1550 x x x x x x x x x x x
1570 x x x x x x
1590 x x x x x x x x x cf.
1610 x x x x x x x x cf. x x
1630 x x x x x x x x x x
1650 x x x x x x
1670 x x x x x x
1690 x x x x
1710 x
1730 x x
1750 x x
1770 x
1790
1810 x x x x
1830 x x x d x x
1850 x x x
1870 x x
1890 x x x x x x x x x
1910 x x x d x x x
1930 x x x x
1950 x x x x
1970 x x x x
1990 x x x d x x x x
2010 x
2030 x x x d x x
2050 x
2070
2090
2110
2130 x
2150 x
2170
2190 x x
2210 x x
2230 x
2250 x
2270
2310 d d d
2330 d
2370
2410
2450
2490 d d
2530
2570
2610
2650
2690
2730
2770
2810
2850
2890
2930
BadenianKarpatianOttnangian
tectonized metamorphic shales
core 2308-2318m
barren
barren
Appendix 1O: Petersdorf deep well 1; distribution of impor-
tant planktonic and benthic foraminifera in the lower part of the well.
914-920 917 x x
924.7-930.8 927.8 x x
933-939
959.5-965.5 1 965
976-982
982-988
988-994
994-1000
1000-1006 contamination
1009-1015
1025.8-1032.0
1043.4-1049.2
1063-1068
1114.3-1120.3
1191-1193
1290.0-1295.7
1352-1354 barren
1397.5-1403,5 contamination
barren
silicified stems
silicified stems
PERBERSDORF 1
Benthic Foraminifera
Core Sample
box number
Sample Depth in Metres
Remarks
Uvigerina pygmoides
Uvigerina macrocarinata
Uvigerina uniseriata
Uvigerina cf. pudica
Uvigerina aculeata
Uvigerina cf. costai
Uvigerina semiornata
Uvigerina grilli
Uvigerina cf. bulbacea
Uvigerina acuminata
Uvigerina graciliformis
Uvigerina parviformis
Uvigerina cf. laviculata
Pappina primiformis
Uvigerina cf. barbatula
Uvigerina sp. (striate)
Vaginulina legumen
Colominella paalzowi
Cylindroclavulina rudis
Psammolingulina papillosa
Pseudogaudryina sturi
Appendix 1N continue
