GeolCarp_Vol59_No5_375

GEOLOGICA CARPATHICA, OCTOBER 2008, 59, 5, 375—394

www.geologicacarpathica.sk

Probing the underground at the Badenian type locality:

geology and sedimentology of the Baden-Sooss section

(Middle Miocene, Vienna Basin, Austria)

MICHAEL WAGREICH

, PETER PERVESLER

, MAKSUDA KHATUN

, INGE WIMMER-FREY

and ROBERT SCHOLGER

Department of Geodynamics and Sedimentology, Center for Earth Sciences, University of Vienna, Althanstrasse 14,

1090 Vienna, Austria; michael wagreich@univie.ac.at

Department of Paleontology, University of Vienna, Althanstrasse 14,1090 Vienna, Austria; peter.pervesler@univie.ac.at

27 Tarington Way NE, Calgary, AB, T3J 4N1, Canada; maksuda.khatun@gmail.com

Geological Survey of Austria, Neulinggasse 38, 1030 Vienna, Austria; i.wimmer-frey@geologie.ac.at

Chair of Geophysics, Paleomagnetic Laboratory Gams, MU Leoben, Austria; robert.scholger@mu-leoben.at

(Manuscript received December 13, 2007; accepted in revised form June 12, 2008)

Abstract: A 102 m long core of fine-grained sediments of the Vienna Basin (Baden Group, “Badener Tegel”) was drilled
at the Badenian type locality outcrop in Baden-Sooss. An Early Badenian age (regional Upper Lagenidae Foraminiferal
Zone) is indicated by biostratigraphy. The core comprises mainly bioturbated, medium to dark grey marls and shales with
a slightly higher degree of tectonic deformation in the upper part of the core. XRD indicates mainly quartz, muscovite/
illite, chlorite, feldspar, calcite and minor dolomite as constituents. Carbonate contents vary between 10 % and 35 % and
organic carbon between 0.32 % and 0.78 %. Rare intercalations include sand layers with shell debris, a conglomerate and
a smectitic tuff layer. Mean grain size ranges from 4 to 8 µm. Cyclic sedimentation was identified by rhythmic variations
in carbonate and organic carbon contents and magnetic susceptibility. Rock Eval pyrolysis indicates mainly type III kero-
gen from terrestrial higher plant material and minor marine input. The depositional environment can be characterized as
offshore, below the fair-weather wave base but within the storm-wave base. The sediments are hemipelagites, transported
by pelagic suspension, that is a mixture of pelagic biogenic carbonate, mainly calcareous nannofossils and foraminiferal
tests, and terrigenous clay and silt. The positive correlation of carbonate to organic carbon indicates a dilution controlled
siliciclastic deposition with varying siliciclastic input. Except for minor primary laminated intervals, oxygenated bottom
water conditions are reconstructed from the presence of various trace fossils and ichnofabrics from the Zoophycos ichnofacies
in the deeper part with a transition to the distal Cruziana ichnofacies towards the top of the core.

Key words: Miocene, Badenian, Vienna Basin, sedimentology, geochemistry, clay mineralogy, hemipelagite.

Introduction

The Neogene Vienna Basin is situated at the junction of the
Eastern Alps and the Western Carpathians, within the territo-
ries of Austria, the Slovak and the Czech Republics (e.g. Wes-
sely 1988; see Fig. 1). The basin has been a classical area of
geological and paleontological investigations of Miocene stra-
ta since the 19

century (e.g. Keferstein 1828; d’Orbigny

1846; Reuss 1848; Hörnes 1856). Numerous studies have
been applied to the deposits and their paleontological content,
also triggered by significant hydrocarbon findings during the
20

century (Hamilton et al. 2000). However, the lack of natu-

ral outcrops restricts detailed sedimentological and paleonto-
logical analysis of Vienna Basin strata to a decreasing number
of active clay pits and quarries.

The fine-grained sediments of the “Badener Tegel” of Mid-

dle  Miocene  age  constitute  a  classical  lithofacies  type  of  the
Vienna Basin (Keferstein 1828) and yield a wealth of macro-
and  microfossils  (e.g.  d’Orbigny  1846).  Modern  sedimento-
logical  investigations  on  the  “Badener  Tegel”  are  largely
missing because of the lack of suitable outcrops. Supported by
the  Austrian  Science  Fund  FWF-Project  P13743-BIO  “Tem-

poral and spatial changes of microfossil associations and ich-
nofacies in the Austrian marine Miocene” a scientific core has
been  drilled  in  January  to  February  2002,  near  the  western
margin of the southern Vienna Basin (Fig. 1). The drill hole
reached  a  depth  of  102  meters  and  was  cored  throughout.
The  aim  of  this  scientific  borehole  Baden-Sooss  was  a  de-
tailed investigation of freshly cored Badenian sediments at the
type  locality  of  the  Badenian,  the  former  clay  pit  Baden-
Sooss (compare Papp & Steininger 1978; Rögl et al. 2008).
Multidisciplinary  studies  were  applied  for  evaluating  bios-
tratigraphy,  paleoecology,  paleoichnology,  sedimentology,
geochemistry,  magnetostratigraphy  and  magnetic  climate
proxies  such  as  magnetic  susceptibility  (Hohenegger  et  al.
2008). This paper presents data on the geology, sedimentolo-
gy and geochemistry from samples of the core of the scientific
borehole Baden-Sooss.

Geological setting

The scientific borehole Baden-Sooss (Fig. 1) penetrated a

succession of Badenian (Langhian, Middle Miocene; Fig. 2)

376

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

fine-grained  deposits,  starting  from  the  type  section  of  the
Badenian stage, the old brickyard Baden-Sooss to the south of
the  town  of  Baden  (geographic  coordinates  WGS84:  E  016°
13’ 44”, N 47° 59’ 24”) (Papp et al. 1978; see also discus-
sion by Rögl et al. 2008). Thus, the borehole explored the sub-
surface  of  the  stratotype  section  which  was  defined  and
described by Papp & Steininger (1978). The borehole site was
situated some tens of meters to the north of the margin of the
former clay pit (for a detailed geological map of the area in-
cluding the drill site see Rögl et al. 2008: fig. 2). As outcrops
in  this  pit  are  now  limited  due  to  extensive  filling  by  waste
material  and  restricted  to  a  partly  covered  old  pit  face  pre-
served  as  a  natural  monument,  and  hidden  faults  may  be
present between the drill site and the outcrops, the core section
could  not  be  directly  correlated  into  the  stratotype  outcrop.
However,  from  the  geological  data  and  the  dipping  of  the
beds,  it  becomes  clear,  that  the  core  strata  represent  more  or
less  the  direct  substrate  of  the  stratotype,  although  some
meters of strata may be missing due to the above mentioned
reasons. Basinward, according to borehole data given by Brix

& Plöchinger (1988), Badenian fine-grained
strata thicken considerably across synsedimen-
tary normal faults.

The Vienna Basin is a rhomb-shaped SSW-

NNE oriented basin of about 200 km long and
55 km  wide.  The  basin  forms  a  thin-skinned
Miocene  pull-apart  basin  (Royden  1985)  and
constitutes  a  marginal  basin  of  the  Central
Paratethys  (for  paleogeographic  overview  see,
e.g. Rögl 1998, 1999; Hámor 2001; Kvaček et
al. 2006; Strauss et al. 2006). The basin formed
due  to  left-lateral  transtension  and  strike-slip
between  the  Alps  and  the  Carpathians  (e.g.
Ratschbacher et al. 1991; Decker 1996; Hamil-
ton et al. 2000; Hinsch et al. 2005).

Stratigraphy

The stratigraphy of the Vienna Basin has

been  a  subject  of  studies  since  the  nineteenth
century.  Paleontological  monographs  (e.g.
d’Orbigny  1846;  Hörnes  1856,  1870;  Karrer
1867)  were  followed  by  detailed  stratigraphic
analysis (see also Rögl et al. 2008). Grill (1941,
1943)  established  zonations  by  foraminifera,
followed  by  significant  stratigraphic  works
such as those by Papp (1951, 1953) and Stein-
inger & Papp (1979).

Based on these classical works and more re-

cent  publications  (e.g.  Hamilton  et  al.  2000;
Kováč  et  al.  2004;  Strauss  et  al.  2006)  the
evolution  of  the  Vienna  Basin  started  during
the Early Miocene (Eggenburgian—Ottnangian—
Karpatian of Central Paratethys stages) with the
development of a partly non-marine piggy-back
basin  on  top  of  Alpine  thrusts  to  the  northeast
of Vienna (Decker 1996). Sinistral transtension
during the Early/Middle Miocene led to the for-

Fig. 1. Tectonic sketch map of the Vienna Basin (modified from Decker 1996, and
Wagreich & Schmid 2002; Neogene = white) at the junction of the Eastern Alps and
the Western Carpathians (hatched areas) and location of the studied borehole
Baden-Sooss in the surroundings of Sooss and Baden (map modified from Wessely
in Rögl et al. 2008).

mation  of  small-scale,  rapidly  subsiding  lows  and  relatively
stable highs during the Badenian. This first phase of tectoni-
cally controlled subsidence is considered to be a result of the
initial  pull-apart  rifting  stage  (Lankreijer  et  al.  1995).  Depo-
centers of the basin shifted towards the south, being filled by a
large  delta  that  developed  in  its  southern  part.  In  the  Early
Badenian,  NE-SW  oriented  faulting  occurred  on  the  western
margin  of  the  basin.  Marine  transgression  started  during  this
time  and  also  reached  the  southern  part  of  the  basin.  Up  to
3000 m  thick  successions  of  fully  marine  Badenian  marls
characterize the central parts of the basin, whereas delta sands
and limestones were deposited on the basin margins or at shal-
low  depths  during  this  time  (Sauer  et  al.  1992;  Weissenbäck
1996;  Seifert  1996).  During  Sarmatian  and  Pannonian  times,
salinity oscillated and finally decreased, leading to limnic-flu-
vial deposits (Harzhauser & Piller 2005a,b, 2007).

Strauss et al. (2006) divided the Neogene sediments in the

southern Vienna Basin into five Middle and Upper Miocene
3

-order depositional sequences, the Badenian comprising

three of these depositional sequences starting with coarse clas-

377

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

tics and carbonates at the base. The middle part of the Bade-
nian represents a thin lowstand with eroded carbonate material
at the base followed by sand and silt deposition. The upper
part of the Badenian is characterized by sand and clay in the
lower part and carbonates in the upper part (Strauss et al.
2006).

In the central and southern Vienna Basin the Badenian sedi-

ments  are  divided  into  proximal  deltaic  clastics  and  a  distal
basinal  facies,  which  is  characterized  by  sandy  marls  and
clays. On the eastern border of the Vienna Basin and in other
partly  protected  marginal  areas,  corallinacean  limestones
(“Leithakalk”,  e.g.  Strauss  et  al.  2006;  Harzhauser  &  Piller
2007) were deposited during periods of sea-level highstand in
the Badenian.

Widespread fine-grained grey Badenian “basinal” deposits

of the offshore, deeper parts of the basin comprise mixtures of
clay and silt, containing significant amounts of illite, chlorite
and  some  smectite  as  reported  by  Wagner  &  Czurda  (1991).
The  first  descriptions  of  these  fine-grained  sediments  date
back  to  Keferstein  (1828)  who  recognized  grey-bluish  clays
locally  named  “Tegel”  around  the  town  of  Baden.  Later  on,
Papp  &  Steininger  (1978)  described  the  Badenian  sediments
in the framework of the stratotype definition of the Badenian
as  greyish-blue,  plastic  clay  with  a  yellowish  weathering  in
the uppermost portion, including minor sand lenses with mol-
luscs. The clays appear massive to crudely bedded in the out-
crop  and  a  total  of  14  meters  of  section  was  documented  by
Papp & Steininger (1978: fig. 30; see also Rögl et al. 2008).

The lithostratigraphic division of these sediments in the

Austrian part of the basin is still under debate. During the 19

and first half of the 20

century only the term “mariner Tegel

von Baden” or “Badener Tegel” was in use. In the revision of
Austrian  Neogene  stratigraphic  nomenclature  for  the  marine
Middle Miocene sediments of the Vienna Basin by Papp et al.
(1968), the stratigraphic term “Badener Serie” as a formation
(Baden Formation) has been introduced but a clear differentia-
tion between litho-, bio-, and chronostratigraphy was not pro-
vided. The recent lithostratigraphic chart of Austria (Piller et
al.  2004)  places  the  “Badener  Tegel”  into  the  Baden  Group,
which can be subdivided into the Jakubov Formation and the
Lanžhot Formation in the Slovak part of the basin (Kováč et
al.  2004).  The  lower  part  of  the  Badenian  including  the
Baden-Sooss core may thus be correlated to the Lanžhot For-
mation.

Biostratigraphic investigations on foraminifera (mainly

lower part of the local Upper Lagenidae Zone, see Hoheneg-
ger  et  al.  2008a)  and  calcareous  nannoplankton  (standard
Zone NN5, see Ćorić & Hohenegger 2008) indicate an Ear-
ly  Badenian  (Langhian)  age  (Fig. 2).  Hohenegger  et  al.
(2008a) dated the core by cyclostratigraphy and orbital tun-
ing to  —14.379 ± 1 and —14.142 Myr ± 9 kyr.

The succession at Baden-Sooss was correlated to the lower-

most 3

-order sequence of the Badenian in the Vienna Ba-

sin, sequence VB5 of Kováč et al. (2004) or Ba1 of Strauss
et  al.  (2006).  Trangressive  conglomerates  form  the  base  of
this  sequence.  The  top  of  this  sea-level  cycle  is  associated
with  a  major  sea-level  drop  throughout  the  Vienna  Basin
(e.g. Weissenbäck 1996), which was correlated with a world-
wide  drop  in  sea  level  from  14.2  to  13.8 Ma  including  the

Fig. 2. Lower to Middle Miocene stratigraphic chart based on the
time scale of Lourens et al. (2004); the black star denotes approxi-
mate stratigraphic position of the Baden-Sooss core based on cyclo-
stratigraphy according to Hohenegger et al. (2008a). Abbreviations of
local zones: UL-Z = Upper Lagenidae Zone, Aggl.F.-Z = Zone of ag-
glutinated foraminifera, Buli-Bo-Z = Bulimina-Bolivina Zone.

Fig. 3. Photograph of drilling equipment (February 2002) at Baden-
Sooss and position near northern margin of the former clay pit.

378

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

Fig. 4. Detailed sedimentological log of the Baden-Sooss core from 7 m to 102 m.

379

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

Lan2/Ser1 sequence boundary of Hardenbol et al. (1998; see
Strauss et al. 2006 and Harzhauser & Piller 2007). However,
the correlation of these regional sea-level cycles to the global
sea-level curve still remains debateable.

Material and methods

Drilling the uppermost 8 meters delivered gravel and loose

pebbles of probable Quaternary age. Cores with a diameter of
15 cm were taken continuously from 8 to 102 m. After split-
ting the core vertically and smoothing the cross-section a thor-
ough  digital  documentation  was  performed  by  whole  core
scanning and digital photography (see Appendix 1A—I). These
image  series  were  also  used  for  the  ichnological  analysis.  A
sedimentological  log  of  the  core  was  documented  by  visual
analysis, forming the base for further investigations and sam-
pling (Fig. 4).

Half of the split core was preserved and stored at the De-

partment  of  Paleontology,  University  of  Vienna.  The  second
half  was  used  as  a  source  of  samples  for  sedimentology,
geochemistry,  microfossils,  nannofossils  and  paleomagnetic
analysis. Trace fossils were detected from 8 to 102 meters core
depth. Additional cuts were made horizontally to the bedding.

For representative grain size analysis, wet sieving and X-ray

sedigraph  techniques  have  been  applied.  Five  representative
samples  were  taken  from  the  Baden-Sooss  core  at  depths  of
20—20.10 m,  40.35—40.45 m,  60.05—60.15 m,  80.20—80.30 m,
100.15—100.25 m. The samples were crushed and dried. Each
sample  was  prepared  by  adding  distilled  water  containing
0.5%  sodium  hexametaphosphate,  disaggregated  for  24 hrs
and  analysed.  The  Sedigraph  5000  ET  produced  measure-
ments for sediments of a grain size smaller than 70 µm. Coars-
er fractions were sieved using a sieve at  > 63 µm prior to the
sedigraph measurements. The relative proportions of the sand,
silt and clay fractions were determined. Various statistical pa-
rameters for grain size interpretation were calculated.

Overview carbonate and organic carbon analyses were per-

formed  on  a  set  of  22  core  samples  from  5 m  intervals.  De-
tailed  carbonate  and  organic  carbon  analyses  were  measured
on 310 samples collected from 40 to 102 m depth (sample in-
terval 20 cm). Calcium carbonate was analysed using the car-
bonate  bomb  technique  of  Müller  &  Gastner  (1971).  Pow-
dered  samples  of  1 g  were  dissolved  in  15%  hydrochloric
acid. Carbonate dissolved and the pressure of the evolved CO

gas were measured and converted to percentages of CaCO

us-

ing calibration curves. Each sample was measured at least two
times. The error of the result is  ± 0.5 %. For analysis of organ-
ic  carbon  contents,  the  same  sample  sets  were  dried  at  room
temperature  prior  to  grinding  with  a  powder  grinding  mill.
The  standard  procedure  involves  heating  the  weighted  dry
sediment  samples  to  550 °C  and  measuring  the  combustion
product  CO

gases by gas chromatography using a LECO

RC-412 device.

The same samples analysed for organic carbon were used

for  Rock  Eval  pyrolysis  (laboratories  of  Baseline  Resolution
Inc. Shenandoah, Texas). The ground rock samples were heat-
ed  in  an  inert  gas  atmosphere  at  a  programmed  rate  while
amounts  of  volatile  hydrocarbons  (S1),  and  of  hydrocarbons

(S2) and CO

(S3) released from the kerogen were measured.

The amount of hydrocarbons (mgHC/g rock) released from
kerogen during heating was normalized against TOC, to give
the Hydrogen Index (HI; Espitaliè et al. 1977). The tempera-
ture at which the maximum release of hydrocarbons occurred
(T

max

) was also recorded as a maturation indicator.

For a geochemistry scan by routine XRF analysis, the over-

view  samples  with  a  sample  distance  of  5 m  were  used.  The
same sample set was used for mineralogy and clay mineralogy
analysis  by  XRD.  The  bulk  and  clay  mineralogy  of  20  core
samples at a 5 m interval was determined by XRD. For bulk
mineral  analysis  the  dried  samples  were  ground  and  loaded
into a sample holder as a randomly oriented powder. Diffrac-
tion data were collected with a Philips X’Pert Multi Purpose
Diffractometer  (goniometer  PW  3050),  Cu-K

α radiation

(40 kV, 40 mA), automatic divergence slit, 0.30 mm receiving
slit, step scan (step size 0.02° 2

Θ ι second per step). The sam-

ples were run from 2—65° 2

Θ. The semiquantitative mineral-

ogical composition was obtained using a computer program
(Paktunc 1998) incorporating information from bulk chemical
analyses.

For clay mineral analysis the samples were treated with

in order to remove organic matter and with ultrasound

for further disaggregation. The < 2 µm fractions were separat-
ed by centrifugation. The clay fractions were saturated with
1 N KCl-solutions and 1 N MgCl

-solutions by shaking 24 h

and  afterwards  washed  in  distilled  water.  Oriented  prepara-
tions  of  the  < 2 µm  fractions  were  achieved  by  suction  of
25 mg clay in suspension on a porous ceramic plate and dry-
ing  at  room  temperature.  Oriented  XRD  mounts  were  then
analysed in the air dried, ethylene glycol, dimethylesulfoxide,
glycerol,  300°  and  550 °C  treated  states.  The  clay  samples
were  run  from  2—50°  2

Θ with the same step and counting

time as the bulk samples. The identification of clay minerals
was carried out according to Moore & Reynolds (1997).

Various rock magnetic investigations were performed on

the core (for details see Selge 2005). Here, only magnetic sus-
ceptibility measurements are reported and evaluated (see also
Hohenegger et al. 2008a). Laboratory measurements were per-
formed  on  standard  paleomagnetic  sample  cubes  for  uncon-
solidated rocks (sampling interval between 25 and 70 cm). All
laboratory magnetic measurements were carried out in the Pa-
leomagnetic  Laboratory  Gams  of  the  University  of  Leoben
(Austria). The measurements included volume- and mass-spe-
cific  susceptibility  and  anisotropy  of  magnetic  susceptibility
(AMS). Magnetic volume susceptibility was furthermore mea-
sured on the full length of the drill core with an Exploranium
KT9 susceptibility-meter. The measurements were performed
at 5 cm point distances to produce a continuous susceptibility
log of the core.

Lithology and log

In general the Baden-Sooss core displays a higher degree of

tectonic  deformation  in  the  upper  40  meters  (Fig. 4  and
Appendix 1A—C).  This  penetrative  deformation  is  recogniz-
able by the presence of some small-scale fault planes, which
show  vertical  throws  of  a  few  mm  to  cm  (Appendix 1A—C).

380

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

Fault planes often appear darker due to concentration of clay
minerals  on  the  surfaces.  These  more  intensely  deformed
rocks can thus be classified as protocataclasites. Despite small
displacements the lithology itself is not strongly influenced by
these tectonic deformations. Below 40—45 m, the fault planes
die  out  completely.  Tectonic  deformation  is  interpreted  as  a
result of a young set of faults connected to a major fault in the
nearby  stratotype  Baden-Sooss  which  displaces  Badenian
against Sarmatian strata (Papp & Steininger 1978).

On the basis of visual investigations four general lithofacies

have  been  recognized  in  the  Neogene  part  of  the  core  below
8 m (Fig. 5). Fine-grained marls and clays (“Badener Tegel”)
constitute  more  than  95 %  of  the  core  (Fig. 5a).  Most  of  the
core marls are bioturbated, only a few intervals of laminated
marls and clays occur (Fig. 5c; see also Appendix 1H). Sand
layers are minor ( < 5 % of the total core log) and often strong-
ly bioturbated; rare mollusc shells are present in such coarser
layers  (Appendix 1A).  An  intraformational  conglomerate  oc-
curs  at  around  27 m  (Fig. 5d;  see  also  Appendix 1B),  and  a
light  grey  5 cm  tuff  layer  is  present  at  72.5 m  (Fig. 5b).  No
regular  variations  in  lithofacies  or  general  trends  along  the

core length have been recognized, except that sand layers are
slightly more common in the upper part of the core.

Sedimentology

Within the marl lithofacies, bioturbation is extremely com-

mon and dense, obliterating most primary sedimentary struc-
tures except for a few short intervals in the lower part of the
core around 80 to 85 m (Fig. 5c). There, primary light-dark
horizontal laminations of lower flow regime origin are (partly)
preserved, although thin section analysis indicates the pres-
ence of some micro-burrows also in these laminated layers.

Due to bioturbation (see Appendix 1), detailed investiga-

tions  on  ichnofossils  and  ichnofabric  analysis  were  essential
for the interpretation of the depositional environment and the
recognition of changes in ecological parameters like oxygen-
ation, nutrients, stability of the environment and the substrate
(see Pervesler et al. 2008). Trace fossils from the ichnogenera
Asterosoma,  Chondrites,  Nereites,  Ophiomorpha,  Phycosi-
phon,  Scolicia,  Siphonichnus,  Teichichnus,  Thalassinoides,

Fig. 5. Typical facies of the Baden-Sooss core: a – bioturbated marl facies, mainly Phycosiphon (core 17.0 m); b – bioturbated tuff layer
(core 72.4 m); c – laminated facies (core 84.5 m); d – intraformational conglomerate (core 22.0 m).

381

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

Trichichnus  and  Zoophycos  were  distinguished  in  cross-sec-
tion.  Phycosiphon  and  Nereites  are  the  most  common  trace
fossils  observed  in  most  horizons.  Asterosoma,  Trichichnus
and Zoophycos are important elements of the deeper parts in
the core; Thalassinoides filled with slightly coarser sediment
occurs in the higher parts from 65 to 8 meters. The co-occur-
rence of certain trace fossils made clustering into several ich-
nofabric types supposable (Pervesler et al. 2008).

Grain size analyses

The analysed grain size of the marls from the Baden-Sooss

core did not indicate any significant trend from bottom to
top of the core (Fig. 6a). The sediment is dominated by par-
ticles smaller than 2 µm (53 %) and particles ranging from

2—44.42 µm  (45 %),  which  corresponds  to  the  clay  and  fine/
medium-sized  silt  fractions.  Very  small  portions  (1.5 %)  of
the sediments range into the fine sand size fraction. The terna-
ry diagram plot of the different fractions of the sediments indi-
cates mainly silty clay (Fig. 6b). They basically bear a pelitic
texture  and  the  size  trends  (Table 1)  are  mainly  bimodal  ex-
cept  in  the  sample  from  40 m  (polymodal)  and  80 m  (trimo-
dal).  The  sample  from  80 m  represents  the  lower  part  of  the
core which comprises light-dark laminated intercalations. The
mean grain size falls into fine silt and clays with median val-
ues (Folk & Ward 1957) from 4 to 6 µm. The sample at 40 m
also  contains  a  significant  proportion  (17 %)  of  coarse  silt.
The sorting is rather poor for all the samples (Table 1) and can
be classified as poorly sorted to very poorly sorted according
to the classification of Folk & Ward (1957). Skewness is sym-

Sample meter

20 m

40 m

60 m

80 m

100 m

SAMPLE TYPE

Bimodal,

poorly sorted

Polymodal, very

poorly sorted

Bimodal,

poorly sorted

Trimodal,

poorly sorted

Bimodal,

poorly sorted

Mean

8.065

11.35

10.24

9.656

9.765

Sorting

8.669

14.14

12.57

12.77

11.44

Skewness 1.947 1.634 1.925

2.106

1.849

METHOD OF
MOMENTS
Arithmetic
(µm)

Kurtosis

7.338 4.789 6.252

6.756

6.260

Mean 4.690

6.386

5.413

4.559

5.623

Sorting 3.175

4.559

3.722

3.516

3.754

Skewness

–0.043

0.027

0.093

0.102

–0.004

FOLK AND
WARD
METHOD
(µm)

Kurtosis

0.896 0.841 0.929

0.986

0.893

Mean 7.736

7.291

7.529

7.777

7.474

Sorting 1.667

2.189

1.896

1.814

1.908

Skewness

0.043

–0.027

–0.093

–0.102

0.004

FOLK AND
WARD
METHOD
(

φ)

Kurtosis 0.896 0.841 0.929

0.986

0.893

Mean

Fine silt

Sorting

Poorly sorted

Very poorly sorted

Poorly sorted

Skewness

Symmetrical

Symmetrical Coarse

skewed Symmetrical

FOLK AND
WARD
METHOD
(Description)

Kurtosis Platykurtic

Platykurtic

Mesokurtic

Platykurtic

Table 1: Grain size characteristics of the Baden-Sooss core, parameters according to method of moments (e.g. Blott & Pye 2001) and Folk
& Ward (1957).

Fig. 6. (a) Grain size cumulative frequency curves and (b) position of samples in a ternary classification diagram Sand—Silt—Clay.

382

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

metrical except at 80 m which shows a coarse skewness. Kur-
tosis is platykurtic or mesokurtic. The samples plot into the
field of pelagic suspension transport (VIII) according to the
CM-diagram (Fig. 7) of Passega (1964).

Carbonate contents

In the 22 overview samples the carbonate values vary from

11 % to 25 % of the total weight (Fig. 8a). Two large cycles
are  visible  even  in  this  coarse  sample  resolution  (see  Ho-
henegger  et  al.  2008a).  Carbonate  values  increase  from  the
bottom of the section up to a maximum value of 25 % at 50 m,
then values decrease again from 40 m up to the top. The high
resolution  analysis  (20 cm  sample  distance  from  40—102 m
core) illustrates that the percentage of carbonate content varies
from 10 % to 35 % (Fig. 8b). In average, the content is 18 %
within this 60 m thick succession. A clear cyclicity including
6 cycles within the lower part of the section can be recognized
by moving average conversion (Fig. 8c).

Organic carbon contents

Organic carbon varies from 0.32 % to 0.78 % of the total

weight along with fluctuations of carbonate contents
(Fig. 9a,b). The percentage starts with the highest values of
around 0.78 % at 95 m depth of the section, and then oscillates
between values below and above 0.60 % (Fig. 9a). A general
trend from slightly higher to lower values from bottom to top
of the section is recognized. The fluctuation of the distribution
of organic carbon throughout the section (Fig. 9b,c) indicates
a cyclic pattern (see Hohenegger et al. 2008a). No distinct or-
ganic carbon peak is associated with the laminated part of the
core at around 84.5 m.

org

—CaCO

curves

The carbonate (CaCO

)

and organic carbon (C

org

) contents

of the Baden-Sooss core were plotted in C

org

—CaCO

dia-

grams to evaluate the basic sediment flux and depositional

Fig. 7. Position of samples in Passega’s (1964) CM-diagram.

model in the pelagic/hemipelagic carbonate-siliciclastic-or-
ganic carbon three-component system (see Ricken 1991,
1993). The diagram (Fig. 10) shows a linear positive relation
between C

org

and CaCO

which indicates a dilution controlled

siliciclastic  deposition  sensu  Ricken  (1993),  that  is  varying
fine-grained siliciclastic input (mainly clay minerals and silt-
sized quartz) controls the facies and cyclicity of the sediments,
whereas  the  carbonate  production  stays  fairly  constant.  The
slope of the regression line of the dilution is moderately slop-
ing,  an  indication  of  a  small  to  moderate  supply  of  organic
matter in the background sediments. According to this model,
decreasing  amounts  of  organic  carbon  and  carbonate  in  the
sediment result from an increase in siliciclastic input and, con-
sequently, indicate an increase in sedimentation rate. Detailed
regression lines for various parts of the core display linear re-
lationships (see Khatun 2007). Organic matter flux was limit-
ed to a threshold value around 0.8 % C

org

. A slight change in

deposition at depths of 55 to 70 m and at 70 to 85 m was rec-
ognized due to a flatter regression line from 55 to 70 m (Kha-
tun 2007).

Type of organic matter based on Rock Eval pyrolysis

Rock Eval pyrolysis is used to identify the type and maturi-

ty of organic matter and to assess petroleum potential in sedi-
ments (e.g. Espitaliè et al. 1977) and can also be useful for pa-
leoenvironmental  reconstruction.  The  relatively  high  organic
content of the Baden-Sooss core and the episodic lamination
made us interested in learning more of the origin of the organ-
ic  matter.  The  hydrogen  index  (HI)  offers  a  way  to  estimate
relative  amounts  of  marine  and  terrestrial  components  build-
ing up the sedimentary organic matter. HI is the ratio of S2 to
TOC  given  in  milligrams  of  hydrocarbons  for  1 g  organic  C
(mg HC/g TOC). HI values range in general from around 30
to  a  maximum  of  90  (Table 2),  typical  for  type  III  kerogen
which  derived  mainly  from  terrestrial  higher  plant  material
and  only  minor  marine  input,  which  is  also  indicated  by  the
HI-OI diagram (Fig. 11). Rock Eval T

max

values range around

410 to 425 with a maximum of 441 which indicates mainly im-
mature conditions of the organic matter (Espitaliè et al. 1977).

Bulk geochemistry, mineralogy and clay

mineralogy

Geochemical analysis for main elements largely corroborat-

ed the carbonate data given above. Although the geochemical
composition of the samples is rather uniform (Table 3), sam-
ples rich in carbonate naturally have slightly lower silica val-
ues and vice versa. SiO

content ranges from 49.5 to 54.5 %.

Outstanding is the tuff layer with a value of 57 %. CaO con-
tent ranges from 7.5% to 11.0 %; again the tuff layer shows a
significantly different value of 4.2 %. Trace elements are also
rather uniform throughout the core and show no significant
variations. Even within the laminated part of the core around
85 m no concentration of anoxia-related elements like vanadi-
um could be recognized (Table 3). The tuff naturally shows
significant discrepancies, for example lower barium, chromi-
um, strontium, and vanadium contents.

383

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

Fig. 8. Carbonate con-
tents  from  (a)  whole
core  overview  sam-
ples,  and  (b)  detailed
sampling  from  40  to
102 m. (c) moving av-
erage  (sample  interval
=  15)  shows  cyclicity
of the data.

Fig. 9. Organic carbon
contents

from

(a)

whole  core  overview
samples,  and  (b)  de-
tailed  sampling  from
40  to  102 m.  (c)  mov-
ing average (sample in-
terval  =  15)  shows  cy-
clicity of the data.

Fig. 10. C

org

—CaCO

scatter diagram for the samples 40—102 m of

the Baden-Sooss core displaying linear regression line.

The results of overview XRD analyses are shown in Fig. 12.

Quartz, albite, muscovite/illite, chlorite, kaolinite, calcite and
dolomite are the main mineral constituents. Pyrite is identified
in all samples. The bulk mineralogy within the profile is rather
uniform. The mineralogy of the samples was calculated on the
basis  of  the  geochemical  bulk  composition  using  the  methods
of Paktunc (1998). This indicates around 30 % of quartz, below
10 % of albite, 15—20 % of muscovite/illite, 10—15 % chlorite,
10  to  15 %  of  kaolinite,  and  15—25 %  of  carbonate  including
dolomite. Decreasing amounts of carbonate correspond to an in-
crease  of  siliciclastic  components.  Systematic  variation  in  the
relative  abundance  of  any  other  mineral  group  was  not  ob-
served. The clay minerals are considered to be detrital and sup-
plied from the same source area of bedrocks and soils.

384

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

Depth

TOC S1 S2 S3 T

max

(m) (wt.

%) (mg/g) (mg/g) (mg/g) (

C) (mg/g)

40.01 0.401 0.05 0.17 0.50  436  42.4
41.21 0.506 0.09 0.19 0.60  428  37.5
42.61 0.535 0.10 0.33 0.98  429  61.7
43.81 0.581 0.12 0.28 1.10  433  48.2
45.01 0.543 0.11 0.33 0.90  434  60.8
46.41 0.498 0.08 0.18 0.83  430  36.2
47.61 0.456 0.07 0.15 0.73  441  32.9
48.81 0.484 0.15 0.34 0.86  424  70.2
50.01 0.579 0.09 0.27 0.70  418  46.7
52.61 0.551 0.23 0.50 0.73  427  90.8
53.81 0.525 0.10 0.27 0.57  432  51.4
54.41 0.541 0.06 0.24 0.99  426  44.4
55.01 0.522 0.18 0.34 0.72  424  65.2
56.41 0.554 0.12 0.34 0.73  419  61.4
57.61 0.507 0.09 0.25 0.68  417  49.3
58.81 0.483 0.10 0.28 0.63  415  58.0
60.01 0.541 0.10 0.22 0.56  416  40.7
61.41 0.539 0.09 0.16 0.66  408  29.7
62.61 0.535 0.11 0.36 0.59  417  67.3

63.815

0.560

0.09

0.28

0.73

417

50.0

65.01 0.608 0.10 0.33 0.84 429 54.3

66.415

0.574

0.10

0.18

1.02

415

31.4

67.61 0.552 0.12 0.34 0.78  426  61.6
68.81 0.593 0.18 0.29 0.67  417  48.9
70.01 0.631 0.18 0.45 0.57  414  71.4

71.415

0.539

0.15

0.33

0.57

416

61.3

72.61 0.482 0.11 0.31 0.58  414  64.4
73.81 0.556 0.08 0.25 0.60  415  45.0
75.03 0.582 0.15 0.45 0.58  422  77.4
76.41 0.535 0.12 0.35 0.77  424  65.4
77.61 0.459 0.08 0.17 0.51  437  37.1
77.63 0.459 0.10 0.30 0.57  415  65.4
78.81 0.567 0.12 0.37 0.66  423  65.3
78.83 0.567 0.12 0.32 0.63  419  56.4
80.01 0.540 0.16 0.36 0.40  401  66.7
81.41 0.485 0.15 0.38 0.68  411  78.4
82.61 0.567 0.08 0.32 0.95  434  56.5

83.815

0.439

0.05

0.15

0.59

409

34.2

84.385

no data

0.08

0.21

0.70

426

no data

84.415

0.480

0.09

0.28

0.70

419

58.3

85.03 0.545 0.09 0.31 0.63  416  56.9
86.43 0.502 0.05 0.23 0.50  412  45.9
87.63 0.651 0.03 0.22 0.78  420  33.8
88.83 0.524 0.05 0.20 0.90  418  38.2
90.01 0.586 0.11 0.42 0.65  421  71.7
91.43 0.604 0.03 0.24 0.90  428  39.7
92.64 0.570 0.04 0.34 0.82  423  59.7
93.83 0.547 0.07 0.39 0.73  419  71.4
95.03 0.564 0.09 0.47 0.54  416  83.3
95.43 0.629 0.07 0.44 0.67  423  70.0
96.23 0.665 0.05 0.38 0.89  420  57.2
96.43 0.617 0.08 0.35 0.79  429  56.8

97.235

0.643

0.08

0.48

0.74

417

74.7

97.63 0.650 0.07 0.45 0.81 424 69.3
98.03 0.644 0.10 0.56 0.67 424 87.0

100.01

0.661

0.12

0.55

0.73

423

83.2

101.03

0.611

0.09

0.46

0.68

424

75.3

101.43

0.553

0.07

0.25

0.75

426

45.2

101.63

0.634

0.08

0.26

0.90

420

41.0

Table 2: TOC and Rock Eval data from 40—102 m of the Baden-Sooss core.

The clay minerals of the < 2 µm fraction comprise abundant

illite/muscovite associated with fairly abundant amounts of
chlorite and kaolinite. A low intensity, broad peak at angles
between 3 and 4.2° 2

Θ indicates the presence of a mixed lay-

er, which could not be further identified. Smectite abundance

varies most. A decrease upward can be recognized
from a maximum at 70 to 75 m to accessory amounts
in the upper 50 m of the section. The clay mineralogy
of the tuff layer is dominated by low charged smectite
with traces of illite, chlorite and kaolinite. Small
amounts of quartz, albite, calcite, dolomite and pyrite
occur in the bulk mineralogy.

Magnetic susceptibility

Selge (2005) recognized mixed assemblages of mul-

tiple magnetic fractions in the core samples with dif-
ferent  grain  sizes  and  mineralogy  such  as  magnetite,
maghaemite,  hematite,  goethite,  and  pyrite.  The  re-
sults of thermomagnetic investigations indicated mag-
netite  as  the  dominant  magnetic  phase  in  all  studied
samples with additional presence of varying amounts
of hematite (for details see Selge 2005). Magnetic sus-
ceptibility measured on the full length of the core indi-
cated cyclic variations with a highly significant large
scale  cycle  of  about  40 m  and  small  scale  cycles  of
about 20, 15 and 11 m in thickness (Fig. 13 and Ho-
henegger et al. 2008a). Peaks in magnetic susceptibili-
ties were linked to higher concentration of hematite re-
lated  to  higher  sediment  influx  as  a  consequence  of
higher  seasonal  contrasts  (cold  winters  and  hot  sum-
mers).  These  enhanced  climate  variations  resulted  in
higher  rates  of  physical  weathering  and  erosion  and,
consequently,  a  higher  amount  of  detrital  magnetic
particles deposited in the basin (Selge 2005; Hoheneg-
ger et al. 2008a).

Discussion

The lithofacies and biofacies of the marls and clays

of the Badenian stratotype were interpreted by Papp &
Steininger (1978) as a shallow-water, fully-marine,
basinal fine-grained facies of water depths around 50—
100 m. Sand and shell layers were interpreted as high-
er energy layers transported from more nearshore en-
vironments to the west into the calm depositional
environment (Papp & Steininger 1978).

According to our investigations, the Baden-Sooss

core strata were deposited within a quiet offshore dep-
ositional environment as proven by the predominance
of fine silt and clay grain sizes of the typical “Badener
Tegel”. Depositional waterdepths were situated below
the fair-weather wave base as no structures indicative
of wave agitation have been found. Bioturbation is
common, also characteristic for moderately deep envi-
ronments below the normal wave base (see Pervesler
et al. 2008). The poor sorting indicated by grain size

analysis may be mainly a result of strong bioturbation. The
fine median values from grain size analysis and the CM-plots
indicate transport and sedimentation from pelagic suspension;
no evidence for turbiditic transport for these fine-grained sedi-
ments is present.

385

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

Sample from
core meter

7 m

10 m

15 m

20 m

25 m

30 m

35 m

40 m

45 m

50 m

55 m

SiO

53.0

54.5

54.0

54.5

53.0

50.0

53.5

52.5

50.0

52.0

TiO

0.743 0.773 0.726 0.764 0.732 0.665 0.679 0.734 0.740 0.686 0.694

15.90 16.50 15.50 16.40 15.10 13.75 14.10 15.70 15.70 14.45 14.47

4.80 4.60 4.40 4.50 4.40 4.00 4.40 4.50 4.80 4.20 4.00

MnO

0.048 0.059 0.051 0.054 0.045 0.047 0.050 0.066 0.064 0.053 0.050

MgO

2.10 2.00 2.10 2.00 2.15 2.10 2.25 2.45 2.05 2.00 2.20

CaO

8.50 7.50 8.30 7.60 8.00 10.50 11.00 8.50 9.00 11.00 10.50

0.80 1.17 1.16 1.19 1.12 1.32 1.11 1.03 1.37 1.08 1.17

2.53 2.70 2.39 2.69 2.41 2.19 2.39 2.54 2.54 2.32 2.34

110 °C

1.36 1.31 1.28 1.37 1.25 0.99 1.08 1.24 1.19 1.17 1.19

0.103 0.113 0.099 0.151 0.095 0.077 0.106 0.095 0.122 0.116 0.104

9.10 8.40 9.60 8.90 9.70 10.80 12.30 8.80 9.80 12.60 11.20

1.12 0.40 0.32 0.50 0.45 0.46 0.33 0.60 0.25 0.45 0.29

total

100.11 100.03 99.92 100.12 99.95 99.90 99.80 99.75 100.12 100.13 100.21

256

279

259

281

270

233

269

290

277

266

276

117

134

140

137

130

145

142

134

132

124

117

128

142

126

142

128

109

121

128

135

119

121

251

227

255

260

254

278

311

276

278

292

328

133

145

127

148

136

104

119

129

138

129

119

163

162

186

152

181

190

169

180

160

158

178

total

1311

1376

1347

1409

1354

1285

1371

1406

1398

1338

1375

Sample from
core meter

60 m

65 m

70 m

75 m

80 m

85 m

90 m

95 m

100 m

Tuff

SiO

51.5

52.0

51.0

49.5

53.0

51.0

49.5

52.0

57.0

TiO

0.708 0.695 0.666 0.698 0.688 0.748 0.730

0.697 0.727 0.411

14.97 14.77 14.33 15.03 14.97 15.91 15.33

14.95 15.64 18.48

4.10 4.40 4.00 4.20 4.70 4.50 4.10

4.30 4.20 3.65

MnO

0.044 0.049 0.045 0.049 0.054 0.062 0.052

0.048 0.050 0.022

MgO

2.13 2.16 2.16 2.30 2.27 2.39 2.13

2.24 2.35 2.23

CaO

10.00 9.60 10.50 9.80 10.30 8.15 9.85

10.50 9.00 4.20

1.20 1.15 1.43 1.34 1.36 1.28 1.39

1.34 1.32 1.73

2.48 2.41 2.32 2.48 2.48 2.68 2.56 2.49 2.60 1.35

110 °C

1.20 1.28 1.30 1.19 1.16 1.21 1.21 1.24 1.24 5.64

0.137 0.096 0.100 0.097 0.119 0.103 0.120 0.139 0.125 0.049

10.90 11.00 11.85 11.35 12.20 9.70 11.00 12.10 10.50 4.90

0.50 0.46 0.50 0.53 0.38 0.29 0.42 0.60 0.42 0.32

total

99.86 100.07 100.20 100.05 100.18 100.02 99.88 100.14 100.18 99.97

291

295

277

290

305

316

320

305

312

189

113

123

124

130

125

132

117

125

131

126

124

118

127

130

142

134

131

136

360

331

334

309

337

282

324

347

313

285

128

115

123

124

133

139

142

132

139

163

175

177

172

150

159

150

159

165

total

1433

1410

1393

1408

1430

1441

1462

1443

1447

1048

Table 3: Main element (in weight %) and trace element (in ppm) geochemistry of samples from the Baden-Sooss core.

Ubiquitous bioturbation generally indicates oxic bottom

water  conditions  except  for  minor  primary  laminated  inter-
vals, which can be related to dysoxic conditions. The laminae
are  partly  disturbed  by  trace  fossils  due  to  subsequent  im-
provement  of  oxygenation  and  burrowing.  The  trace  fossil
Scolicia,  produced  by  stenohaline  irregular  echinoids,  indi-

cates  full  marine  conditions  (e.g.  Bromley  &  Asgaard  1975;
Smith  &  Crimes  1983).  The  salinity  tolerant  crustacean  bur-
row Thalassinoides (Frey et al. 1984) replaces Scolicia in the
higher  portions  of  the  core.  The  presence  of  Zoophycos  and
associated  Phycosiphon,  Nereites  and  Teichichnus  suggests
the Zoophycos ichnofacies for the deeper part of the core. Up

386

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

Fig. 11. Hydrogen Index (HI) versus Oxygen Index (OI) diagram
based on Rock Eval analysis for samples from 40—102 m; kerogen
types I—IV based on Espitaliè et al. (1977).

Fig. 12. Bulk mineral composition of 20 core samples and the tuff layer.

the core, Thalassinoides is more common. This may suggest a
transition to the distal Cruziana ichnofacies. Such a relation
indicates shallowing up to the upper offshore zone (cf. Pem-
berton et al. 2001) or at least a higher clastic input.

The percentage of carbonate of 10 % and 35 % indicates the

presence of marls. XRD analysis shows mainly calcite, dolo-
mite contents are rather low in percentage. The carbonate con-
tents in such a fully marine, deeper-water setting may include
the following constituents:

• Pelagic carbonate from the tests of mainly planktonic,

carbonate secreting organisms (mainly calcareous nanno-
plankton and foraminifera);

• Reworked extra-basinal carbonate from the erosion of

carbonate rocks in the hinterland of the basin;

• Minor constituents include carbonate from shells and tests

of benthic organisms (e.g. molluscs, foraminifera) and authi-
genic carbonate precipitated on the sea floor or during diagen-
esis.

The main carbonate constituents as seen in the Baden-Sooss

core  samples  are  calcareous  nannofossils,  planktonic  and
benthic  foraminifera  (see  Ćorić  &  Hohenegger  2008)  and
some mollusc shells. Presence of extra basinal, reworked car-
bonate could be excluded or is at least below 10 % in the fine-
grained  parts  of  the  core,  due  to  the  lack  of  significant
amounts of dolomite. Thus, the ‘Baden Tegel’ can be classi-
fied  as  a  hemipelagite,  namely  a  mixture  of  mainly  pelagic

387

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

Fig. 13. Magnetic susceptibility, measured on the core (

core

) and on

subsamples (

); the SIRM ratios describe the relative contributions of

high-coercive to low-coercive magnetic phases (for details see Selge
2005). Cycle peaks (grey) identified by high values of susceptibility.

biogenic carbonate and terrigenous clay and silt. The presence
of  muscovite  and  chlorite  in  the  clay  mineral  suite  points  to
significant  amounts  of  metamorphic  source  areas,  that  is  the
Austroalpine basement units to the south and east of the Vien-
na  Basin.  No  systematic  variations  in  the  length  of  the  core
have been recognized in the composition of the detrital frac-
tion, indicating neither provenance changes nor major climate
changes during this interval.

The organic matter fraction of fine-grained sediments can

be composed of organic particles of various sources, including
imported  terrestrial  plant  matter  and  matter  primarily  pro-
duced in the marine environment. The accumulation of organ-
ic  matter  in  depositional  environments  is  controlled  by  three
main  variables:  rates  of  production,  destruction,  and  dilution
(Bohacs et al. 2005). The distribution and concentration of or-
ganic carbon through the analysed core indicates that organic
matter flux was limited to a threshold value below 0.8 % C

org

Consequently, the rates of production of organic matter were
comparatively low. The whole data set generally follows a di-
lution controlled siliciclastic flux model (sensu Ricken 1993)
with moderate to low levels of production and minor destruc-
tion of organic matter.

This depositional type, characterized by varying siliciclastic

input, suggests a hemipelagic, oxic environment. No signs for
anoxia were found even in laminated parts of the core. The hy-
drogen index and oxygen data of Rock Eval analysis mainly
suggest a terrestrial plant material source for the organic mat-
ter mixed with marine organic matter. The hydrogen index
versus oxygen index plot demonstrates kerogen type III,
though a very few samples show a minor tendency for type II
kerogen of marine production. The plot also indicates an im-
mature stage of hydrocarbon generation.

The low slope or flatness of the carbonate-organic carbon

regression lines support the interpretation of a varying silici-
clastic  dominated  background  sedimentation  with  minor  ad-
mixtures  in  pelagic  biogenic  carbonate.  The  siliciclastics  are
derived from continental fluvial input into the basin. Periods
with high carbonate production are predominantly associated
with higher oxygenation at the sediment surface, expressed in
a decreasing supply of organic matter. Decreasing amounts of
organic  carbon  and  carbonate  in  the  sediment  suggest  an  in-
crease in the sedimentation rate (Ricken 1996).

The results presented can also be interpreted in terms of

subtle variations in relative sea level and productivity. Inter-
vals with lower carbonate contents might represent regression-
al or sea-level lowstand phases characterized by low calcare-
ous productivity and high siliciclastic dilution. These could be
associated with higher runoff from the rising orogenic hinter-
land. Times of high sea level may thus result in lower silici-
clastic dilution and higher plankton productivity.

Infrequent sand and shell layers, also strongly bioturbated,

record the effect of higher energy events, probably storms, and
thus can be interpreted as tempestites transported from near-
shore or deltaic environments to the west. They may also rep-
resent distal pro-delta sand layers (comp. Wessely et al. 2007).
Due to the lack of primary sedimentary structures both inter-
pretations are still valid; deposition above or within the storm
wave base can be assumed due to the presence of shell lags.
The slight increase in number of sand layers towards the upper

388

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

part of the core indicates shallowing or a higher sand input. A
slight shallowing in the uppermost part of the section is also
indicated  by  the  increase  in  number  of  macrofossil  lenses  as
described  from  the  stratotype  section  (Papp  &  Steininger
1978) and is corroborated by the trace fossil record (Pervesler
et al. 2008) and foraminiferal assemblages (Hohenegger et al.
2008b).  A  general  shallowing  trend  in  largely  coeval  Bade-
nian sediments was also recorded a few kilometers further to
the south, at Bad Vöslau (Wessely et al. 2007).

Rare events disturbing the generally quiet offshore sedimen-

tation of fine-grained sediments include a debris flow con-
glomerate bed in the upper part of the core. This submarine
mass flow may have been triggered by seismic shocks due to
earthquakes at nearby synsedimentary basin margin faults. A
tuff layer in the lower part of the core testifies to the presence
of coeval volcanism some distance away from the Vienna Ba-
sin (see, e.g. Handler et al. 2006).

Conclusion

From grain size analysis and geochemical data of the

Baden-Sooss core at the type locality of the Badenian we con-
clude that the fine-grained bioturbated deposits of the southern
Vienna Basin were deposited in a quiet offshore environment
below  the  fair  weather  wave  base.  A  pelagic  autochthonous
carbonate  fraction,  mainly  calcareous  nannofossils  and  fora-
minifera, and a terrigenous clay and fine silt fraction form the
marls  of  the  “Badener  Tegel”.  Cyclic  sedimentation  was
mainly due to variance in the siliciclastic input, that is dilution
cycles due to siliciclastic-dominated flux. Organic matter de-
rived  mainly  from  terrigenous  input  of  higher  land  plants.  A
slight shallowing is recorded from the lower to the upper part
of the core.

Acknowledgments: The study was supported by the Austrian
Science  Fund  (FWF,  Projects  P13743-BIO,  P13740-GEO,
P18203-N10  and  P16793-B06).  We  thank  Alfred  Uchman,
Katalin  Báldi,  Stjepan  Ćorić,  Fred  Rögl,  Christian  Rupp,
Anna Selge, Robert Scholger and Karl Stingl for assistance and
helpful  discussions.  We  thank  the  technical  staff  of  the  De-
partment  of  Paleontology,  University  of  Vienna,  for  trans-
porting  and  cutting  the  core.  We  thank  Maria  Fencl  for
preparation of sedimentological logs. We thank the reviewers
of the manuscript for suggestions and improvements.

References

Blott S.J. & Pye K. 2001: Gradistat: a grain size distribution and

statistics package for the analysis of unconsolidated sediments.
Earth Surf. Process. Landforms 26, 1237—1248.

Bohacs K.M., Grabowski G.J., Carroll A.R., Mankiewicz P.J., Mis-

kell-Gerhardt  K.J.,  Schwalbach  J.R.,  Wegner  M.B.  &  Simo
J.A.  2005:  Production,  destruction,  and  dilution  –  the  many
paths  to  source-rock  development.  In:  Harris  N.B.  (Ed.):  The
deposition  of  organic-carbon-rich  sediments:  models,  mecha-
nisms, and consequences. SEPM Spec. Publ. 82, 61—101.

Brix F. & Plöchinger B. 1988: Erläuterungen zu Blatt Wiener Neus-

tadt. Geol. Bundesanst., Wien, 1—85.

Bromley R.G. & Asgaard U. 1975: Sediment structures produced by

a spatangoid echinoid: a problem of preservation. Bull. Geol.
Soc. Denmark 24, 261—281.

Ćorić S. & Hohenegger J. 2008: Quantitative analyses of calcareous

nannoplankton assemblages from the Baden-Sooss section
(Middle Miocene of Vienna Basin, Austria). Geol. Carpathica
59, 5, 447—460.

Decker K. 1996: Miocene tectonics at the Alpine-Carpathian junc-

tion and the evolution of the Vienna Basin. Mitt. Gesell. Geol.
Bergbaustud. Österr. 41, 33—44.

d’Orbigny A. 1846: Foraminifères fossiles du Bassin Tertiaire de

Vienne (Autriche). Die fossilen Foraminiferen des tertiaeren
Beckens von Wien. Gide et Comp., Paris, I—XXXVII, 1—312.

Espitaliè J., LaPorte J.L., Madec M., Marquis F., Leplat P., Paulet

J. & Boutefeu A. 1977: Méthode rapide de charactérisation des
roches mères de leur potential pétrolier et de leur degré
d’evolution. Rev. Inst. Francais Pétrole 32, 23—42.

Folk R.L. & Ward W.C. 1957: Brazos River bar (Texas); a study in

the significance of grain size parameters. J. Sed. Petrology 27,
3—26.

Frey R.W., Curran A.H. & Pemberton G.S. 1984: Tracemaking ac-

tivities of crabs and their environmental significance: the ich-
nogenus Psilonichnus. J. Paleontology 58, 511—528.

Grill R. 1941: Stratigraphische Untersuchungen mit Hilfe von Mik-

rofaunen im Wiener Becken und den benachbarten Molasse-
Anteilen. Öl Kohle 37, 595—602.

Grill R. 1943: Über mikropaläontologische Gliederungsmöglich-

keiten im Miozän des Wiener Becken. Mitt. Reichsanstalt für
Bodenforschung 6, 33—44.

Hamilton W., Wagner L. & Wessely G. 2000: Oil and gas in Aus-

tria. Mitt. Österr. Geol. Gesell. 92, 235—262.

Handler R., Ebner F., Neubauer F., Bojar A.-V. & Hermann S.

2006:

Ar/

Ar dating of Miocene tuffs from the Styrian part

of the Pannonian Basin: an attempt to refine the basin stratigra-
phy. Geol. Carpathica 57, 483—494.

Hardenbol J., Thierry J., Farley M.B., Jacquin T., Graciansky P.-C. &

Vail P.R. 1998: Mesozoic and Cenozoic sequence chronostrati-
graphic  framework  of  European  basins.  In:  Graciansky  C.-P.,
Hardenbol  J.,  Jacquin  T.  &  Vail  P.R.  (Eds.):  Mesozoic  and
Cenozoic  sequence  stratigraphy  of  European  basins.  SEPM
Spec. Publ. 60, 3—13.

Harzhauser M. & Piller W.E. 2005a: Neogen des Wiener Beckens.

Exkursionsführer 75. Jahrestagung der Paläontologischen Ge-
sell., Graz, 1—42.

Harzhauser M. & Piller W.E. 2005b: Paratethyan paleogeography

depositional regimes and major sea-level fluctuations. Excur-
sion A., 12

Congress R.C.M.N.S., 6.—11. September 2005,

Vienna, 6.—11., Vienna.

Harzhauser M. & Piller W.E. 2007: Benchmark data of a changing

sea – Palaeogeography, palaeobiogeography and events in the
Central Paratethys during the Miocene. Palaeogeogr. Palaeo-
climatol. Palaeoecol. doi:10.1016/j.palaeo.2007.03.031.

Hámor G. 2001: Explanatory notes to the Miocene palaeogeograph-

ic maps of the Carpathian Basin. Geol. Inst. Hung., Budapest,
1—71.

Hinsch R., Decker K. & Wagreich M. 2005: 3-D mapping of seg-

mented active faults in the southern Vienna Basin. Quart. Sci.
Rev. 24, 321—336.

Hohenegger J., Ćorić S., Khatun M., Pervesler P., Rögl F., Rupp C.,

Selge A., Uchman A. & Wagreich M. 2008a: Cyclostratigraph-
ic dating in the Lower Badenian (Middle Miocene) of the Vien-
na Basin (Austria) – the Baden-Sooss core. Int. J. Earth Sci.

DOI 10.1007/s00531-007-0287-7.
Hohenegger J., Andersen N., Báldi K., Ćorić S., Pervesler P., Rupp

C. & Wagreich M. 2008b: Paleoenvironment of the Early Bad-
enian (Middle Miocene) in the southern Vienna Basin (Aus-

389

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

tria) – multivariate analysis of the Baden-Sooss section. Geol.
Carpathica 59, 5, 461—487.

Hörnes M. 1856: Die fossilen Mollusken des Tertiärbeckens von

Wien (Gastropoden). Abh. Geol. Reichsanst. Wien 3, 1—404.

Hörnes M. 1870: Die fossilen Mollusken des Tertiärbeckens von

Wien (Bivalven). Abh. K.K. Geol. Reichsanst. Wien 4, 1—279.

Karrer F. 1867: Zur Foraminiferenfauna in Österreich. Sitz.-Ber.

K.K. Akad. Wiss., Math. Naturwiss. Cl. 55, 331—368.

Keferstein C. 1828: Beobachtungen und Ansichten über die geog-

nostischen Verhältnisse der nördlichen Kalk-Alpenkette in
Oesterreich und Baiern. Teutschland Geognostisch-Geol.
Dargestellt 5, (3), 1—425.

Kováč M., Baráth I., Harzhauser M., Hlavatý I. & Hudáčková N.

2004: Miocene depositional systems and sequence stratigraphy
of the Vienna Basin. Cour. Forsch.-Inst. Senckenberg 246,
187—212.

Kvaček Z., Kováč M., Kovar-Eder J., Doláková N., Jechorek H.,

Parashiv V., Kováčová M. & Sliva . 2006: Miocene evolution
of landscape and vegetation in the Central Paratethys. Geol.
Carpathica 57, 4, 295—310.

Lankreijer A., Kováč M., Cloetingh S., Pitoňák P., Hlôška M. &

Biermann C. 1995: Quantitative subsidence analysis and for-
ward modelling of the Vienna and Danube basins; thin-skinned
versus thick-skinned extension. Tectonophysics 252, 433—451.

Lourens L., Hilgen F., Shackleton N.J., Laskar J. & Wilson D.

2004: The Neogene Period. In: Gradstein F.M., Ogg J.G. &
Smith A.G. (Eds.): A geologic time scale 2004. Cambridge
Univ. Press, 409—440.

Moore D.M. & Reynolds R.C. 1997: X-ray diffraction and the iden-

tification and analysis of clay minerals. 2

Edition. Oxford

University Press, New York, 1—378.

Müller G. & Gastner M. 1971: The “Karbonat-Bombe,” a simple

device for the determination of the carbonate content in sedi-
ments, soils and other materials. Neu. Jb. Mineral., Mh. 10,
466—469.

Paktunc A.D. 1998: Modan: an interactive computer program for

estimating mineral quantities based on bulk composition: win-
dows version. Computers and Geosciences 24, 425—431.

Papp A. 1951: Das Pannon des Wiener Beckens. Mitt. Geol. Gesell.

39—41 (1946—48), 99—193.

Papp A. 1953: Die Molluskenfauna des Pannon im Wiener Becken.

Mitt. Geol. Gesell. 44, 85—222.

Papp A. & Steininger F. 1978: Holostratotypus des Badenien. Ho-

lostratotypus: Baden-Sooss (südlich von Wien), Niederösterre-
ich, Österreich. Badener Tegel—Keferstein, 1828 (Unterbaden;
M4b; Obere Lagenidenzone). In: Papp A., Cicha I., Seneš J. &
Steininger F. (Eds.): Chronostratigraphie und Neostratotypen:
Miozän der Zentralen Paratethys. Bd. VI. M

Badenien (Mora-

vien, Wielicien, Kosovien). VEDA SAV, Bratislava, 138—145.

Papp A., Grill R., Janoschek R., Kapounek J., Kollmann K. & Tur-

novsky K. 1968: Zur Nomenklatur des Neogens in Österreich
– Nomenclature of the Neogene of Austria. Verh. Geol.
Bundesanst. 1968, 9—27.

Papp A., Cicha I., Seneš J. & Steininger F. (Eds.) 1978: Chrono-

stratigraphie und Neostratotypen: Miozän der Zentralen Para-
tethys. Bd. VI. M

Badenien (Moravien, Wielicien, Kosovien).

VEDA SAV, Bratislava, 1—594.

Passega R. 1964: Grain size representation by CM patterns as a geo-

logic tool. J. Sed. Petrology 34, 830—847.

Pemberton S.G., Spila M., Pulham A.J., Saunders T., MacEachern

J.A., Robbins D. & Sinclair I.K. 2001: Ichnology and sedimen-
tology of shallow to marginal marine systems. Geol. Assoc.
Canada, Short Course Notes 15, 1—343.

Pervesler P., Uchman A. & Hohenegger J. 2008: New methods for

ichnofabric analysis and correlation with orbital cycles exem-
plified by the Baden-Sooss section (Middle Miocene, Vienna

Basin). Geol. Carpathica 59, 5, 395—409.

Piller W.E., Egger H., Erhart C., Gross M., Harzhauser M., Hub-

mann B., van Husen D., Krenmayr H.-G., Krystyn L., Lein R.,
Lukeneder A., Mandl G., Rögl F., Roetzel R., Rupp C., Schna-
bel W., Schönlaub H.P., Summesberger H. & Wagreich M.
2004: Die Stratigraphische Tabelle von Österreich 2004 (sedi-
mentäre Schichtfolgen). Österreichische stratigraphische Kom-
mission und Kommission für die paläontologische und
stratigraphische Erforschung Österreichs.

Ratschbacher L., Frisch W., Linzer H.G. & Merle O. 1991: Lateral

extrusion in the Eastern Alps. 2. Structural analysis. Tectonics
10, 257—271.

Reuss A.E. 1848: Die fossilen Polyparien des Wiener Tertiärbeck-

ens. Naturwiss. Abh. von W. Heidinger 2, 1—78.

Ricken W. 1991: Variations of sedimentation rates in rhythmically

bedded sediments. Distinction between depositional types. In:
Einsele G., Ricken W. & Seilacher A. (Eds.): Cycles and
events in stratigraphy. Springer, Berlin, 168—187.

Ricken W. 1993: Sedimentation as a three-component system. Lec-

ture N. Earth Sci. 51, 1—211.

Ricken W. 1996: Bedding rhythms and cyclic sequences as docu-

mented in organic carbon-carbonate patterns, Upper Creta-
ceous, Western Interior, U.S. Sed. Geol. 102, 131—154.

Royden L.H. 1985: The Vienna Basin. A thin-skinned pull-apart ba-

sin. In: Biddle K.T. & Christie-Blick N. (Eds.): Strike slip de-
formation, basin formation and sedimentation. SEPM Spec.
Publ. 37, 319—338.

Rögl F. 1998: Palaeogeographic considerations for Mediterranean

and Paratethys seaways (Oligocene to Miocene). Ann.
Naturhist. Mus. Wien 99A, 279—310.

Rögl F. 1999: Mediterranean and Paratethys, facts and hypotheses

of an Oligocene to Miocene paleogeography (short overview).
Geol. Carpathica 50, 4, 339—349.

Rögl F., Ćorić S., Harzhauser M., Jiménez-Moreno G., Kroh A.,

Schultz O., Wessely G. & Zorn I. 2008: The Middle Miocene
Badenian stratotype at Baden-Sooss (Lower Austria). Geol.
Carpathica 59, 5, 367—374.

Sauer R., Seifert P. & Wessely G. 1992: Guidebook to Excursions

in the Vienna Basin and the adjacent Alpine-Carpathian thrust-
belt in Austria. Mitt. Österr. Geol. Gesell. 85, 1—264.

Seifert P. 1996: Sedimentary-tectonic development and Austrian

hydrocarbon potential of the Vienna Basin. In: Wessely G. &
Liebl W. (Eds.): Oil and gas in Alpidic thrustbelts and basins
of Central and Eastern Europe. EAGE Spec. Publ., (Geol. Soc.
London) 5, 331—341.

Selge A. 2005: Cyclostratigraphy by means of mineralmagnetic pa-

rameters in the middle Badenian (Middle Miocene) core Sooß/
Baden (Vienna Basin, Austria). Unpubl. Dipl. Thesis, Univer-
sity of Leoben, 1—84.

Smith A.B. & Crimes T.P. 1983: Trace fossils formed by heart urchins

– a study of Scolicia and related traces. Lethaia 16, 79—92.

Steininger F.F. & Papp A. 1979: Current biostratigraphic and radio-

metric correlations of Late Miocene Central Paratethys stages
(Sarmatian s.str., Pannonian s.str. and Pontian) and Mediterra-
nean stages (Tortonian and Messinian) and the Messinian
Event in the Paratethys. Newslett. Stratigr. 8, 100—110.

Strauss P., Harzhauser M., Hinsch R. & Wagreich M. 2006: Se-

quence stratigraphy in a classical pull-apart basin (Neogene,
Vienna Basin). A 3D seismic based integrated approach. Geol.
Carpathica 57, 185—197.

Wagner J.-F. & Czurda K.A. 1991: Radionuklidsorption an tertiären

Tonen. Mitt. Österr. Geol. Gesell. 83, 215—227.

Wagreich M. & Schmid H.P. 2002: Backstripping dip-slip fault his-

tories: Apparent slip rates for the Miocene of the Vienna Ba-
sin. Terra Nova 14, 163—168.

Weissenbäck M. 1996: Lower to Middle Miocene sedimentation

390

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

A. Log meters 8 to 20.

model of the central Vienna Basin. In: Wessely G. & Liebl W.
(Eds.): Oil and gas in Alpidic thrustbelts and basins of Central
and Eastern Europe. EAGE Spec. Publ. 5, 255—363.

Wessely G. 1988: Structure and development of the Vienna Basin in

Austria. In: Royden L.H. & Horvath F. (Eds.): The Pannonian

Appendix 1

Basin – a study in basin evolution. Bull. Amer. Assoc. Petrol.
Geol. Mem. 45, 333—346.

Wessely G., Ćorić S., Rögl F., Draxler I. & Zorn I. 2007: Geologie

und Paläontologie von Bad Vöslau (Niederösterreich). Jb. Geol.
Bundesanst. 147, 419—448.

391

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

B. Log meters

20 to 30.

C. Log meters

30 to 40.

392

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

E. Log meters

50 to 60.

D. Log meters

40 to 50.

393

GEOLOGY AND SEDIMENTOLOGY OF THE BADEN-SOOSS SECTION (MIDDLE MIOCENE, AUSTRIA)

F. Log meters

60 to 70.

G. Log meters

70 to 80.

394

WAGREICH, PERVESLER, KHATUN, WIMMER-FREY and SCHOLGER

I. Log meters 90 to 102.

H. Log meters

80 to 90.