GeolCarp_Vol65_No1_55

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GEOLOGICA CARPATHICA

, FEBRUARY 2014, 65, 1, 55—66 doi: 10.2478/geoca-2014-0004

Introduction

In the last decade much work has been done in the Badenian
(e.g. Kováč et al. 2004, 2007; Harzhauser & Piller 2007;
Piller et al. 2007), the first regional stage of the Middle Mio-
cene in the Central Paratethys (Cicha & Seneš 1968; Papp et
al. 1968). However, despite numerous publications, the tim-
ing of the Badenian, its division into substages and their ages
remain vague.

On the basis of wells in the type area of the Badenian, the

Vienna  Basin,  Grill  (1943)  subdivided  the  Badenian,  at  that
time erroneously equalized with the Mediterranean Tortonian
stage, into 4 zones, renamed by Papp & Turnovsky (1953) as
the basal “Lageniden Zone”, the “Sandschaler Zone” (aggluti-
nated  foraminifera  zone),  the  “Bulimina/Bolivina  Zone”  and
the  uppermost  zone  of  impoverished  faunas;  by  definition,
this  was  established  as  a  regional  ecostratigraphic  zonation.
Utilizing  the  evolution  of  the  benthic  foraminifer  Uvigerina,
Papp & Turnovsky (1953) divided the “Lageniden Zone” into
lower  and  upper  parts.  This  division  was  perpetuated  in  the
description of the Badenian stage by Papp et al. (1978a), lead-
ing to the erection of three Badenian substages: Moravian (La-

Timing of the Middle Miocene Badenian Stage of the Central

Paratethys

JOHANN HOHENEGGER

, STJEPAN ĆORIĆ

and MICHAEL WAGREICH

Department of Palaeontology, University of Vienna, A-1090 Wien, Austria; johann.hohenegger@univie.ac.at

Geological Survey of Austria, A-1030 Wien, Austria; stjepan.coric@geologie.ac.at

Department of Geodynamics and Sedimentology, University of Vienna, A-1090 Wien, Austria; michael.wagreich@univie.ac.at

(Manuscript received May 28, 2013; accepted in revised form October 16, 2013)

Abstract: A new and precisely defined chronometric subdivision of the Badenian (Middle Miocene, regional stage of
Central Paratethys) is proposed. This uses global events, mainly geomagnetic polarity reversals as correlated chronometric
boundaries, supported by climatic and sea-level changes in addition to isotope events and biostratigraphic data. The Karpatian/
Badenian boundary lies at 16.303 Ma, at the top of Chron C5Cn.2n, which is near the base of the Praeorbulina sicana
Lowest-occurrence Zone (LOZ). The Badenian/Sarmatian boundary is placed at the top of polarity Chron C5Ar.2n, thus at
12.829 Ma. In relation to three sea level cycles TB 2.3, TB 2.4 and TB 2.5 and astronomically confirmed data, the Badenian
can be divided into three parts of nearly equivalent duration. The Early Badenian as newly defined here ranges from 16.303
to 15.032 Ma (top of polarity Chron C5Bn.2n). The younger boundary correlates roughly to the base of the planktonic
foraminifera Orbulina suturalis LOZ at 15.10 Ma, the HO (Highest Occurrence) of the nannofossil Helicosphaera
ampliaperta at 14.91 Ma (NN4/NN5 boundary) and the Lan2/Ser1 sequence boundary at 14.80 Ma. The subsequent Mid
Badenian ranges from 15.032 Ma to 13.82 Ma; the latter datum correlates with the base of the Serravallian, characterized
by a strong global cooling event reflected in the oxygen isotope event Mi3b. The main part of cycle TB 2.4 falls into the
Mid Badenian, which can be subdivided by a short cooling event at 14.24 Ma during the Middle Miocene Climate Transi-
tion (14.70 to 13.82 Ma). The HCO (Highest common occurrence) of the nannofossil Helicosphaera waltrans at 14.357 Ma
supports this division, also seen in the tropical plankton Zones M6 Orbulina suturalis LOZ and M7 Fohsella peripheroacuta
LOZ that correspond roughly to the lower and upper Lagenidae zones in the Vienna Basin, respectively. The Late Badenian
is delimited in time at the base to 13.82 Ma by the Langhian/Serravallian boundary and at the top by the top of polarity
Chron C5Ar.2n at 12.829 Ma. The Mediterranean Langhian/Serravallian boundary can be equated with the Mid/Late
Badenian boundary at 13.82 Ma. However, the Karpatian/Badenian boundary at 16.303 Ma, a significant event easily
recognizable in biostratigraphy, paleoclimate evolution and sequence stratigraphy, cannot be equated with the proposed
global Burdigalian/Langhian, and thus Early/Middle Miocene boundary, at 15.974 Ma.

Key words: Middle Miocene, Badenian, Paratethys, magnetostratigraphy, biostratigraphy, paleoclimate, sequence
stratigraphy.

genidae zone), Wielician (agglutinated foraminifera zone) and
Kosovian  (Bulimina/Bolivina  zone  and  the  zone  of  impover-
ished  faunas)  in  the  Central  Paratethys  (Papp  et  al.  1978b).
The Moravian was thought to represent the lowermost part of
the Badenian, including the Badenian stratotype (Hohenegger
&  Wagreich  2012).  The  overlying  Wielician  is  characterized
by  widespread  evaporites  in  both  the  Carpathian  Foredeep
(Peryt 2006) and the Transylvanian Basin (Krézsek & Filipescu
2005),  followed  by  the  pronounced  marine  transgression  of
the Kosovian. The Badenian was correlated with the Langhian
and the lower part of the Serravallian by Papp et al. (1978c),
whereas  the  Bulimina/Bolivina  zone  and  the  Kosovian  were
equated to the lower Serravallian (Papp et al. 1978c).

Using the Neogene time-scale of Lourens et al. (2004a)

and Hilgen et al. (2012), the duration and limits of the Bade-
nian substages were linked to the Mediterranean global stages
(Piller  et  al.  2007).  In  these  attempts,  the  Karpatian/Bade-
nian  boundary  was  equated  with  the  Burdigalian/Langhian
boundary at 15.97 Ma (Strauss et al. 2006; Piller et al. 2007).
This date was criticized by Rögl et al. (2007a,b), who put the
boundary at 16.303 Ma, the FAD (First Appearance Date) of
the  foraminifer  Praeorbulina  sicana.  The  Wielician/Koso-

HOHENEGGER, ĆORIĆ and WAGREICH

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GEOLOGICA CARPATHICA, 2014, 65, 1, 55—66

vian  boundary  was  equated  with  the  Langhian/Serravallian
boundary  at  ca.  13.65 Ma  (Piller  et  al.  2007),  based  on  the
ages constraints available before the Serravallian GSSP was
erected  (Hilgen  et  al.  2009).  The  Badenian/Sarmatian
boundary, placed at 12.7 Ma by Harzhauser & Piller (2004)
and Piller et al. (2007), was based on a correlation with se-
quence  stratigraphy  and  the  glacio-eustatic  isotope  event
MSi-3  of  Abreu  &  Haddad  (1998).  In  contrast,  Lirer  et  al.
(2009) used astronomical data to suggest an age of 13.32 Ma
for  this  boundary.  The  Moravian/Wielician  boundary  could
not  be  constrained  with  similar  precision,  but  was  approxi-
mated  to  a  stratigraphic  level  just  after  the  Lan2/Ser1  se-
quence boundary at 14.2 Ma, connected to a significant global
sea-level drop (Strauss et al. 2006) or a more regional, tectoni-
cally influenced sea-level lowstand (Rögl et al. 2007a).

The creation of the Serravallian GSSP at 13.82 Ma (Hilgen

et al. 2009), the search for the GSSP of the Langhian stage,
suggested to lie at the top of the polarity Chron C5Cn.1n at
15.974 Ma (Lourens et al. 2004a,b; Hilgen et al. 2012), and
recently  published  data  mainly  from  the  Vienna  Basin  (e.g.
Kováč  et  al.  2007;  Hohenegger  et  al.  2011;  Hohenegger  &
Wagreich  2012),  the  Styrian  Basin  (e.g.  Schreilechner  &
Sachsenhofer  2007;  Hohenegger  et  al.  2009;  Spezzaferri  et
al. 2009) and the Transylvanian Basin (e.g. de Leeuw et al.
2012) make it necessary to reconsider the ages, delimitations
and subdivisions of the Badenian.

In the following, the Badenian is chronometrically divided

into ages based on astronomically tuned geomagnetic polarity
reversals, paleoclimatic events, biozones and sea-level changes.
This time frame could be the basis for reconsidering the chro-
nostratigraphic substages and their boundary stratotypes.

Methods

In principle, existing data were used for a new “chrono-

metric” (geochronological) subdivision of the Badenian into
ages  defined  by  multistratigraphic  methods.  Consequently,
we use Early, Mid and Late for the chronometric subdivision
of  the  Badenian  (see  recent  discussions  in  Gradstein  et  al.
2012, and Zalasiewicz et al. 2013). Timing and subdivision
rely  primarily  on  magnetostratigraphy  supported  by  bio-
stratigraphic  markers.  Magnetostratigraphy  dates  are  pre-
ferred  because  of  their  global  synchronicity  and  stable  and
high-resolution  dating,  based  on  the  Astronomically  Tuned
Neogene  Time  Scale  (ATNTS,  see  Lourens  et  al.  2004a,b;
Ogg 2012; Gradstein et al. 2012). Numerical ages from geo-
chronology and astrochronology are considered, where appro-
priate, to obtain an improved time frame of geochronological
ages for the proposed subdivisions of the Badenian.

Sequence stratigraphy and isotope stratigraphy (oxygen

isotope  excursions)  are  used  as  secondary  correlation  tools.
In  contrast  to  former  compilations  (e.g.  Piller  et  al.  2007;
Rögl et al. 2007a), sequence stratigraphy is not used here as
the basis for the proposed subdivisions, because of problems
in  exact  timing,  especially  for  unconformities  that  encom-
pass  considerable  time  gaps  at  sequence  boundaries.  They
are  used,  however,  as  additional  means  of  correlation  and
calibration, both to regional and global 3rd-order cycles.

Sequence stratigraphy correlations are based principally

on three sea-level cycles (TB 2.3, TB 2.4 and TB 2.5; Haq et
al.  1988)  recognized  in  the  time  interval  between  the  late
Burdigalian  and  the  late  Serravallian,  which  coincide  with
the Badenian in a broad sense. The sequences in Hardenbol
et  al.  (1998)  concerning  the  Middle  Miocene  are  based  on
seismic  data  from  the  Pannonian  Basin.  Newer  investiga-
tions of global sea-level variation using drill-cores from the
New Jersey and Delaware coastal plains, also detected three
sequences in the interval between 16 Ma and 13 Ma (Miller
et al. 2005a,b; Kominz et al. 2008). These correlate strongly
with  sequences  TB 2.3,  TB 2.4  and  slightly  less  well  with
TB 2.5  in  the  Paratethys,  possibly  marking  the  three  Bade-
nian cycles and sequences in seismic sections (e.g. Strauss et
al. 2006; Schreilechner & Sachsenhofer 2007). The sequence
boundaries of Hardenbol et al. (1998) have to be newly cali-
brated  due  to  the  recently  refined  timing  of  the  Neogene
(Hilgen  et  al.  2012;  Anthonissen  &  Ogg  2012);  as  a  result,
they  have  not  been  used  directly  as  geochronological  con-
straints in our new subdivision of the Badenian based on bio-
stratigraphy and magnetostratigraphy data from classic areas
such as the Vienna Basin.

New Badenian chronometry and subdivision

The Badenian was defined as the first regional stage of the

Middle  Miocene  in  the  Central  Paratethys  by  Papp  et  al.
(1978a),  based  on  the  work  of  Cicha  &  Seneš  (1968)  and
Papp et al. (1968). A threefold division of the Badenian was
suggested and defined by Papp et al. (1978a), including three
stratotypes: (1) Lower Badenian—Moravian, (2) Middle Bad-
enian—Wielician and (3) Upper Badenian—Kosovian. We re-
define  this  subdivision  for  the  Lower  Badenian,  where
considerable shortcomings have been reported in recent years
(e.g. Hohenegger et al. 2009). This new subdivision also dif-
fers from the recent compilations of Krijgsman & Piller (in
Hilgen et al. 2012).

Karpatian/Badenian boundary

Papp & Cicha (1978) defined the base of the Badenian stage

at the first occurrence of the planktonic foraminifer Praeorbu-
lina, which we largely follow here. Since the FAD of Praeor-
bulina sicana was regarded by Cita & Blow (1969) as the base
of the Langhian, thus determining the Lower/Middle Miocene
boundary,  the  Karpatian/Badenian  boundary  was  equated
with  the  Burdigalian/Langhian  boundary.  Berggren  et  al.
(1995)  discussed  the  FAD  of  P.  glomerosa  sensu  stricto  at
16.1 Ma as a possible Langhian boundary marker, due to the
diffuse onset of P. sicana at the type locality (Fornaciari et al.
1997). In terms of nannofossil zonations, the base of the Bade-
nian was originally correlated to nannoplankton Zone NN5 by
Papp  et  al.  (1978c),  and,  more  recently,  placed  in  the  upper-
most NN4 (e.g. Kováč et al. 2004; Rögl et al. 2007a,b; Piller
et al. 2007; Hohenegger et al. 2009).

Depending on different time calibrations of the Praeorbu-

lina lineage, the Karpatian/Badenian boundary, as deter-
mined by the beginning of that lineage, was either set at

TIMING OF THE REGIONAL BADENIAN STAGE (MIDDLE MIOCENE, CENTRAL PARATETHYS)

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16.4 Ma (Ćorić et al. 2004) following the FAD of P. sicana
in Berggren et al. (1995) or 16.303 Ma (Rögl et al. 2007a,b;
Harzhauser & Piller 2007), or at 16.27 Ma (Hohenegger et
al. 2009) according to the FAD of P. glomerosa given in
Lourens et al. (2004b).

Both boundaries differ strongly in age from the Burdiga-

lian/Langhian  boundary,  namely  the  base  of  the  Langhian,
recently proposed at 15.974 Ma, which is the top of polarity
Chron  C5Cn.1n  (Lourens  et  al.  2004a;  Hilgen  et  al.  2012).
This proposal was put forward because the onset of the ex-
tremely  rare,  but  highly  variable  index  fossil  Praeorbulina
sicana (Jenkins et al. 1981; Rio et al. 1997) is blurred in al-
most  all  sections  to  be  considered  for  the  Langhian  GSSP
(Turco  et  al.  2009).  Although  the  top  of  polarity  Chron
C5Cn.1n  is  a  distinct  boundary  in  magnetostratigraphy,  its
calibration by biostratigraphic markers is problematic if the
Globigerinoides—Praeorbulina lineage is not taken into con-
sideration. Using calcareous nannofossils, the HCO (Highest
Common Occurrence) of Helicosphaera ampliaperta and the
beginning of the Paracme Zone of Sphenolitus heteromorphus
have been proposed as biostratigraphic markers approximat-
ing  the  proposed  polarity  chron  boundary  (Iaccarino  et  al.
2009). Both nannofossil markers are not very useful, because
these  events  are  based  on  abundance  peaks  that  may  differ
strongly between regions, due to environmental differences.
Moreover,  the  HO  (Highest  Occurrence)  of  H.  ampliaperta
at  astronomically  calibrated  14.91 Ma  (Shackleton  et  al.
1999)  defines  the  boundary  between  NN4/NN5  (Martini
1971) and can better be used for the division of the Langhian
into an earlier and later part. The abundance peak of H. am-
pliaperta  at  15.899 ± 0.024  Ma  is  in  fact  close  to  the  pro-
posed  boundary,  but  this  peak  is  inconsistent  because  it  is
ecologically controlled as demonstrated by the broad confi-
dence intervals (Abdul Aziz et al. 2008). The much narrower
confidence limits for the base of the Paracme Zone of Sphe-
nolitus  heteromorphus  at  15.949 ± 0.005 Ma  (Abdul  Aziz  et
al. 2008) could be a better signal, but this zone, defined by
the  lack  of  plankton,  is  very  strongly  controlled  by  paleo-
ecology  and  is  thus  of  questionable  value,  especially  when
comparing  different  regions  and  oceans.  For  example,  a
large gap in the distribution of  S. heteromorphus, compara-
ble to a paracme zone, can be detected in the continuous sec-

tion of the Badenian stratotype belonging to the upper La-
genidae zone (Ćorić & Hohenegger 2008).

To clarify the position of the base of the Badenian in rela-

tion to the Burdigalian/Langhian boundary, more continuous
transitions from the Karpatian to the Badenian have been in-
vestigated. So far, such transitions are not known from out-
crops in the Central Paratethys, where unconformities due to
tectonic movements (“Styrian Tectonic Phase”; Stille 1924;
Rögl  et  al.  2007b)  between  Karpatian  and  Badenian  sedi-
ments occurred (see also Rögl et al. 2002). However, investi-
gations of wells in the Alpine Foredeep (Ćorić & Rögl 2004)
and in the Styrian Basin (Hohenegger et al. 2009) documented
the presence of significant intervals of sediment between the
latest Karpatian and the base of the lower Lagenidae zone as
the (former) inferred base of the Badenian. These sediments
represent the time interval between ca. 16.3 Ma (Hohenegger
et  al.  2009)  and  at  least  15.5 Ma,  a  considerable  time  span
that  has  so  far  been  largely  missed  in  Badenian  chrono-
stratigraphy.  This interval correlates with the upper part of
nannoplankton Zone NN4. In wells of the Alpine-Carpathian
Foredeep  the  boundary  between  the  Karpatian/Badenian  is
documented  by  unconformities  with  conglomerates  at  the
base of the overlying successions (Ćorić & Rögl 2004), and
by  an  angular  unconformity  in  2D  seismic  data  from  the
eastern Styrian Basin (Schreilechner & Sachsenhofer 2007).

Looking at the Styrian Basin in more detail (Fig. 1a,b),

this lowermost Badenian, which represents the time interval
between the late Karpatian and the (former) lower Badenian,
is  documented  in  three  outcrop  sections:  the  former  brick-
yard  at  Wagna  (Fig. 2),  the  Retznei  quarry  and  the  former
sand pit at Katzengraben (Hohenegger et al. 2009; Spezzaferri
et al. 2009). A closer look at the Wagna section brings sig-
nificant  arguments  on  the  here  newly  defined  Early  Bade-
nian (Hohenegger et al. 2011) and, thus, the new beginning
of the Badenian.

In the upper part of the Wagna section, the lowermost

Badenian is represented by an 8 m thick section (Fig. 2). De-
tailed sedimentological, magnetostratigraphic, biostratigraphic
(Hohenegger et al. 2009) and paleoenvironmental investiga-
tions  (Spezzaferri  et  al.  2009)  documented  different  phases
in  the  transgression  of  the  Badenian  Sea.  A  significant  un-
conformity  between  silty  sediments  of  the  (Karpatian)

Fig. 1. a – Basins of the Central Paratethys mentioned in the text (modified from Hohenegger & Wagreich 2012). b – Styrian Basin with
the location of Wagna, Retznei, Katzengraben (modified from Hohenegger et al. 2009).

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“Steirischer  Schlier”  and  marly  sand  with  small  pebbles  at
the  base  of    the  overlying  (Badenian)  sequence  could  be
linked  with  the  Styrian  tectonic  phase  (Rögl  et  al.  2007b).
While the Steirischer Schlier biostratigraphically belongs to
the Karpatian according to the planktonic foraminifer Globi-
gerina ottnangiensis and the benthic foraminifera Uvigerina
graciliformis  and  Pappina  primiformis  (Hohenegger  et  al.
2009), the overlying marly sand is characterized by Praeor-
bulina sicana found close to the base of the section part, and
by  a  brackish  water  influence  (Spezzaferri  et  al.  2009).
Depth estimations based on depth ranges of benthic foramin-
ifera  (Hohenegger  2004)  strengthened  the  evidence  for  the
occurrence of a phase of tectonic uplift, from depths around
300 m in the Karpatian to 40 m in the following section in-
terval (Fig. 2). This shift is contemporaneous with a climate
change (Hohenegger et al. 2009), in the form of a significant
warming,  as  documented  in  the  calcareous  nannoplankton
(see  Fig. 2  and  Spezzaferri  et  al.  2009),  and  the  instanta-
neous  drop  in  oxygen  and  carbon  isotope  values  (Latal  &
Piller 2003). This indicates tectonic movements and a coeval
climate/paleoenvironmental change.

Dating of the section following this uplift is based on magne-

tostratigraphy, in combination with biostratigraphic markers

(Fig. 2).  The  section  between  the  two  unconformities  at
20.5 m  and  13.8 m  shows  a  more  or  less  continuous  sedi-
mentation, seen in marly fine sand, interrupted by the growth
of  a  coral  bank.  The  estimated  paleowater-depth  varies  be-
tween 10 m and 40 m. The NN4 index fossil H. ampliaperta
is common throughout this part of the section except in the
coral bank (which provides a striking example for the prob-
lems and chronostratigraphic misuse of an ecologically con-
trolled, regionally restricted Paracme Zone).

The polarity reversal event, from normal to reverse, at

15 m is delimited by two biostratigraphic markers. First, the
reversal falls within nannoplankton Zone NN4 (Martini 1971),
which ends at 14.91 Ma; second, the reversal must be younger
than 16.38 Ma because the occurrence of Praeorbulina sicana
indicates the beginning of plankton Zone M5 (zonation accord-
ing to Wade et al. 2011). Therefore, only two chron boundaries
come into consideration: C5Cn.1n/C5Br at 15.974 Ma, which
has recently regarded as the Burdigalian/Langhian, and
thus the Early/Middle Miocene boundary (see above), and
C5Bn.2n/C5Bn.1r at 15.032 Ma (Hilgen et al. 2012).

The first alternative seems to be more appropriate consid-

ering 3

order sequences established in the Pannonian Basin

(Hardenbol et al. 1998; Vakarcs et al. 1998), because the in-

Fig. 2. Wagna, old brickyard, section 3. Interpreted stratigraphy, based on paleomagnetics, lithology, foraminiferal plankton (Hohenegger et al.
2009) and nannoplankton percentages, combined with depth estimations by benthic foraminifera using the method of Hohenegger (2004).

TIMING OF THE REGIONAL BADENIAN STAGE (MIDDLE MIOCENE, CENTRAL PARATETHYS)

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GEOLOGICA CARPATHICA, 2014, 65, 1, 55—66

terval in question, from 16.40 Ma to 14.80 Ma, is represented
by the single TB 2.3 sea-level cycle (Haq et al. 1988) start-
ing  with  the  Bur5/Lan1  sequence  boundary.  Accepting  the
first  hypothesis,  then  the  C5Cn.1n/C5Br  boundary  falls  ex-
actly within the transgressive phase of this sequence (Fig. 3).
This is confirmed by paleodepth estimates within the Wagna
section (Fig. 2), where the end of the Transgressive Systems
Tract  and  the  beginning  of  the  Highstand  Systems  Tract
(HST)  is  represented  by  the  only  preserved  shallow-water
sediments  between  two  significant  unconformities  ( = se-
quence boundaries), deposited just after the maximum flood-
ing surface (Fig. 2). In the second alternative, the presence of
these shallow water sediments (around 15.032 Ma) is difficult
to explain in a sequence stratigraphy context, because it would
be positioned near the end of the Falling Stage Systems Tract
of the TB 2.3 cycle (Fig. 3), and thus in the strongest erosional
phase as represented by the unconformity. In addition, there is
no  indication  for  tectonic  subsidence  at  that  time  that  could
explain landward extension of shallow-marine sediments in a
Lowstand Systems Tract.

If the Karpatian/Badenian boundary were correlated with

the proposed Burdigalian/Langhian boundary at 15.974 Ma,

then  it  is  recognizable  in  the  Wagna  section  only  by  paleo-
magnetic  data,  because  the  contemporaneous  sedimentary
change from coral limestone to fine sand disappears laterally
within  a  few  meters  (compare  Fig. 4  in  Hohenegger  et  al.
2009).  In  contrast,  the  beginning  of  cycle  TB 2.3  (Haq  et  al.
1988),  at  around  16.4 Ma  (Hardenbol  et  al.  1998),  forms  a
suitable and easily correlated boundary between the Karpatian
and  Badenian  stages.  This  date  marks  the  beginning  of  the
“Middle Miocene Climate Optimum” (Fig. 3; Holbourn et al.
2007)  and  is  correlated  with  the  base  of  the  foraminiferal
plankton  Zone  M5,  the  lowest  occurrence  of  Praeorbulina
sicana (Wade et al. 2011). In addition to this definition based
on  sequence  stratigraphy,  paleoclimate  and  biostratigraphy,
the Styrian tectonic phase documented by a strong uplift and
the subsequent deepening led to the first Badenian transgres-
sion (Hohenegger et al. 2009). Therefore, we place the Karpa-
tian/Badenian  boundary  at  16.303 Ma,  the  top  of  C5Cn.2n
(ATNTS 2012, Hilgen et al. 2012) near the beginning of the
Praeorbulina  lineage  (16.38 Ma;  Wade  et  al.  2011;  Antho-
nissen & Ogg 2012); this confirms the original definition by
Papp  &  Cicha  (1978).  This  boundary  definition  and  age,  as
defined by magnetostratigraphy, was also used by Kováč et al.

Fig. 3. Timing of the Badenian based on magnetostratigraphy, foraminiferal plankton and nannoplankton stratigraphy, 3

order sequences,

sea-level changes in the NW Atlantic and stable oxygen isotopes in the eastern tropical Pacific.

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GEOLOGICA CARPATHICA, 2014, 65, 1, 55—66

(2007), Harzhauser & Piller (2007), Oszczypko & Oszczypko-
Clowes (2012) and Hohenegger & Wagreich (2012).

Thus the ecologically, climatologically and tectonically

well  defined  Karpatian/Badenian  boundary  does  not  corre-
late  with  the  proposed  Burdigalian/Langhian  boundary,  de-
fined  by  the  top  of  polarity  Chron  C5Cn.1n  at  15.974 Ma
(Lourens et al. 2004a; Hilgen et al. 2012); the latter does not
show a significant ecological, environmental and climate sig-
nal  (Fig. 3).  This  proposed  Burdigalian/Langhian  boundary
does not justify a clear differentiation between Early and Mid-
dle  Miocene,  which  should  be  documented  in  strong  climate
changes  reflected  in  the  macro-  and  microfauna  (Harzhauser
& Piller 2007).

Badenian/Sarmatian boundary

The end of the Badenian, the start of the Sarmatian, as de-

fined by a major turnover in faunal elements (e.g. Harzhauser
&  Piller  2004),  is  extremely  controversial  in  its  timing,
which  ranges  in  the  Central  Paratethys  from  an  astronomi-
cally  dated  13.32 Ma  (Lirer  et  al.  2009)  to  12.7 Ma
(Harzhauser & Piller 2004; Piller et al 2007; Paulissen et al.
2011).  Restricted  connections  to  the  open  oceans  are  corre-
lated  to  sea-level  lowstands  such  as  the  glacio-eustatic  iso-
tope event MSi-3 (Abreu & Haddad 1998) at 12.7 (Piller et
al. 2007). The benthic foraminiferal

O Mi4 event was also

suggested  as  a  possible  Badenian/Sarmatian  boundary  and
tentatively  recalibrated  to  12.8 Ma  by  Turco  et  al.  (2001;
13.00 Ma  of  Westerhold  et  al.  2005)  following  Lourens  &
Hilgen (1997).

Paulissen et al. (2011) used well data in the central part of

the  Vienna  Basin  to  tentatively  correlate  the  Badenian/Sar-
matian boundary (at 12.7 Ma) to the top of C5An.1n, but indi-
cated poor resolution and difficulties in a reliable correlation
in the Badenian up to the boundary interval. De Leeuw et al.
(2012)  dated  the  boundary  in  the  Transylvanian  Basin  at
12.80 Ma, within C5Ar.2r. However, their uncertainty inter-
val  ranges  from  12.68  to  12.84 Ma,  including  the  tops  of
C5Ar.1n,  C5Ar.2r  and  C5Ar.2n  of  ATNTS  (Lourens  et  al.
2004a; Ogg 2012). Selmeczi et al. (2012) investigating wells
from  Western  and  Northern  Hungary  by  magnetostratigra-
phy and biostratigraphy reinforced the estimation by Lirer et
al. (2009) placing the boundary at 13.15 Ma.

To find appropriate boundaries, correlations between se-

quence  cycles,  magnetostratigraphy  and  biostratigraphic
data  are  necessary.  The  largest  part  of  the  Late  Badenian
can be correlated with the third sea-level cycle (TB 2.5 after
Haq et al. 1988) that must be calibrated to newer time scales.
To  overcome  these  problems,  and  in  accordance  with  our
previous  approach,  we  use  a  magnetostratigraphic  defini-
tion  as  a  synchronous  event  for  the  base  of  the  Sarmatian
around the 12.7—12.8 Ma datum suggested by several previ-
ous  authors.  We  suggest  placing  the  Badenian/Sarmatian
boundary  at  12.829 Ma,  which  is  the  top  of  polarity  Chron
C5Ar.2n  (Ogg  2012).  This  datum  is  near  to  the  suggested
boundary  age  of  previous  studies  (Piller  et  al.  2007;  De
Leeuw et al. 2012, 2013), correlates well with the Mi4 dating
in Turco et al. (2001) and follows the lowest sea-level stand
in the NW Atlantic (Kominz et al. 2008), approximating the

Ser3 sequence boundary of Hardenbol et al. (1998) at ca.
12.7 Ma (Fig. 3; 12.72 Ma according to TS Creator Vers. 6.1,
http://www.tscreator.org).

Early Badenian

The beginning of the Early Badenian, here dated at 16.303

Ma, corresponds roughly to the base of foraminiferal plank-
ton  Zone  M5,  the  Praeorbulina  sicana  LOZ  (Wade  et  al.
2011;  Anthonissen  &  Ogg  2012).  The  Bur5/Lan1  sequence
boundary  estimated  at  ca.  16.4 Ma  (Hardenbol  et  al.  1998,
TS  Creator  Vers.  6.1,  http://www.tscreator.org)  is  close  to
this limit (Fig. 3).

The end of the Early Badenian corresponds to the top of

polarity  Chron  C5Bn.2n  at  15.032 Ma  (Lourens  et  al.
2004b). We chose this age because it best approximates the
base  of  plankton  Zone  M6,  the  Orbulina  suturalis  LOZ
(Wade et al. 2011) at 15.10 Ma, the calcareous nannoplank-
ton boundary NN4/NN5 (Martini 1971; Anthonissen & Ogg
2012)  positioned  at  14.91 Ma,  and  to  the  Lan2/Ser1  se-
quence boundary at ca. 14.8 Ma (Hardenbol et al. 1998). The
newly  defined  Early  Badenian  therefore  has  a  duration  of
1.271 million years.

From a sequence stratigraphical viewpoint, the Early Bad-

enian  is  represented  by  sea-level  cycle  TB 2.3  (Haq  et  al.
1988) (Fig. 3). According to the revised planktonic foramin-
iferal biostratigraphy calibrated by geomagnetic polarity and
the astronomical time scale, the Early Badenian corresponds
to  the  Subzone  M5b,  the  Praeorbulina  sicana  Lowest  Oc-
currence  Zone  between  16.38  (Anthonissen  &  Ogg  2012)
and 15.10 Ma (Wade et al. 2011; Anthonissen & Ogg 2012).
Paleoclimatically, the Early Badenian for the most part coin-
cides with the “Middle Miocene Climate Optimum” (Phase 1
in Holbourn et al. 2007; for Central Paratethys paleoclimate
records – see – e.g.  Harzhauser  &  Piller  2007;  Harzhauser
et al. 2011) starting with an increase in temperature at 16.5 Ma
and keeping constant temperatures until 14.7 Ma (Shevenell et
al. 2004; Holbourn et al. 2004, 2007; Fig. 3).

Sediments of this first Badenian sea-level cycle are diffi-

cult  to  identify  in  outcrops  and  were  commonly  strongly
eroded  away  due  to  the  Styrian  tectonic  phase,  before  the
more  significant  Mid  Badenian  transgression.  Where  the
sediments are preserved in the shallower areas of the Styrian
Basin,  the  sequence  boundary  Lan2/Ser1  is  easily  recog-
nized  by  strong  erosion  (Rögl  et  al.  2002).  Nevertheless,
the  Early  Badenian  time  is  represented  in  deeper  parts  of
the Styrian Basin by subsurface sediments found as 250 to
750 m  thick  drill  sections  in  the  Western  Styrian  Basin
(Hohenegger  et  al.  2009)  and  as  the  first  Badenian  se-
quence  in  2D  seismic  data  from  the  Eastern  Styrian  Basin
(Schreilechner & Sachsenhofer 2007). Karpatian and Early
Badenian  sediments  are  largely  uniform  in  wells  of  the
Styrian  Basin,  both  indicating  deeper  marine  sedimenta-
tion, but they are separated by an unconformity that reflects
the  Styrian  Tectonic  Phase  in  deeper  parts  of  the  Styrian
Basin. The upper limit of the first Badenian cycle is docu-
mented  as  a  sequence  boundary  in  the  Styrian  Basin  with
continuous  and  conformable  deeper  water  sedimentation
(Schreilechner & Sachsenhofer 2007).

TIMING OF THE REGIONAL BADENIAN STAGE (MIDDLE MIOCENE, CENTRAL PARATETHYS)

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GEOLOGICA CARPATHICA, 2014, 65, 1, 55—66

In the Austrian part of the Alpine-Carpathian Foredeep,

the  first  Badenian  transgression,  coupled  with  the  Styrian
Tectonic  Phase,  is  documented  in  deep  wells  such  as
Roggendorf-1  by  basal  transgressive  conglomerates  below
the Grund Formation (Ćorić & Rögl 2004). Subsurface sedi-
ments show a 90 m thick clastic sequence of Early Badenian
age that overlies the silty-marly Laa Formation of Karpatian
age (Ćorić & Rögl 2004). This section is unconformably fol-
lowed  by  basal  conglomerates  with  fine  sediments  of  the
Grund  Formation  of  Mid  Badenian  age.  The  upper  limit  of
the first Badenian cycle is marked by a clastic influence and
the interval includes the sudden disappearance of H. amplia-
perta (top of NN4).

Analogous to this succession, the 200 m thick Iváň Forma-

tion, a submarine canyon fill in the Moravian part of the Al-
pine-Carpathian  Foredeep,  unconformably  overlies  the
Karpatian Laa Formation (Nový Přerov Member). The canyon
fill shows a similar sequence of basal clastic sediments over-
lain by clays, dated as 16.5—16.3 Ma (Dellmour & Harzhauser
2012).  This  member  is  separated  from  the  overlying  Mid
Badenian sediments by an unconformity (Adámek et al. 2003)
and is regarded as Early Badenian (according to our definition)
in contrast to Dellmour & Harzhauser (2012). The basal silici-
clastic sediments underlying the Grund Formation in the Car-
pathian  Foredeep  of  Moravia  represent  the  Early  Badenian
according  to  the  nannoflora  (Švábenická  2002;  Tomanová-
Petrová & Švábenická 2007).

In the inner part of the Polish Carpathian Foredeep, Karpa-

tian  alluvial  fans  are  overlain  by  the  Dębowiec  conglomer-
ates,  deposited  during  the  first  Badenian  transgression,
passing  upwards  into  dark,  clayey-sandy  sediments  of  the
Skawina Formation (Oszczypko & Oszczypko-Clowes 2012).
Praeorbulina  glomerosa  indicates  that  the  lower  part  of
these up to 1000 m thick sediments belong to the Early Bad-
enian,  while  the  Mid-Badenian  transgression,  indicated  by
O. suturalis in the upper part of the Skawina Formation, fills
the  outer  part  of  the  Carpathian  Foredeep  with  the  upper
Skawina  Formation  and  the  Baranów  Beds  (Oszczypko  &
Oszczypko-Clowes 2012).

In the north-western Transylvanian Basin, the Karpatian

fan deltas and their overlying erosional surfaces are overlain
in  the  shallower-water  parts  of  the  basin  by  conglomerates
and thence by fine siliciclastic deposits containing the index
fossil  P.  glomerosa.  In  the  deeper-water  parts  of  the  basin,
the  fine  siliciclastics  of  Early  Badenian  age  directly  overlie
the basement (Krézsek & Filipescu 2005). This Early Bade-
nian transgression is defined by Krézsek & Filipescu (2005)
as TST1 in the sequence stratigraphy. This is followed by the
second Badenian transgression (TST2) after HST1 and LST2
initiating the newly defined Mid Badenian, with O. suturalis
marking  its  beginning.  De  Leeuw  et  al.  (2012)  dated  this
event in the Transylvanian Basin as older than the Dej Tuff
Complex;  that  is,  older  than  14.38 Ma,  consistent  with  our
geochronological correlations.

Mid Badenian

We propose that the beginning of the Mid Badenian be

fixed at 15.032 Ma, at the top of polarity Chron C5Bn.2n

(Lourens et al. 2004b; Ogg 2012). This is slightly above the
base of plankton Zone M6, the Orbulina suturalis LOZ
(Wade et al. 2011).

According to the orbitally-based time calibration of the

Badenian stratotype at its type locality (Baden Sooss), the in-
terval  between  13.982 Ma  and  13.964 Ma  (Hohenegger  &
Wagreich  2012)  belongs  to  the  upper  Lagenidae  zone,  and
hence  the  end  of  the  Mid  Badenian  has  to  be  younger.  The
next significant event is the climatically controlled Langhian/
Serravallian  boundary  at  13.82 Ma  (Hilgen  et  al.  2009),
within  the  upper  part  of  magnetochron  C5ACn.  Therefore,
the Mid Badenian as defined here spans the time interval be-
tween 15.032 and 13.82 Ma, with a duration of 1.212 million
years (Fig. 3).

There is a clear climatic transition from the “Middle Mio-

cene  Climate  Optimum”  lasting  until  14.7 Ma  (Phase I  in
Holbourn  et  al.  2007)  to  the  subsequent  “Middle  Miocene
Climate  Transition”  (Phase II)  between  14.7  and  13.82 Ma,
characterizing  the  main  part  of  the  Lagenidae  zone,  and  is
thus Mid Badenian in age. The world-wide extreme tempera-
ture  decrease  at  13.82 Ma  led  to  lower,  continuously  de-
creasing  temperatures  in  the  following  Phase III,  termed
“Icehouse” by Holbourn et al. (2007), and a significant glo-
bal sea-level drop which also affected the Paratethys (e.g. de
Leeuw et al. 2010).

The strong transgression of the Paratethys Sea, character-

ized by the appearance of the planktonic foraminifera Prae-
orbulina  circularis  and  Orbulina  suturalis  together  with
the  nannoplankton  Helicosphaera  waltrans,  Sphenolithus
heteromorphus and the absence of H. ampliaperta, was for-
merly  believed  to  be  the  first  Badenian  transgression  (Rögl
et al. 2002). According to the LO (lowest occurrence) of O.
suturalis  at  15.10 Ma  (Wade  et  al.  2011)  and  the  HO  of  H.
ampliaperta  at  14.91 Ma  (Lourens  et  al.  2004b),  this  trans-
gression must lie close to the base of Zone NN5 (Fig. 3). It
marks the onset of sea-level cycle TB 2.4 (Haq et al. 1988)
starting with the Lan2/Ser1 sequence boundary, estimated by
Hardenbol et al. (1998) to lie at 14.8 Ma. The TB 2.4 cycle
ends  with  the  Ser2  boundary,  dated  to  around  13.6 Ma
(Hardenbol  et  al.  1998;  13.54 Ma  according  to  TS  Creator
Vers. 6.1, http://www.tscreator.org). Thus cycle TB 2.4 mostly
represents  the  former  “lower”  Badenian,  but  now  the  Mid
Badenian according to our subdivision (see also Piller et al.
2007). This Mid Badenian is subdivided in the Vienna Basin
into the lower and upper Lagenidae zones (Fig. 3).

The division of the Mid Badenian based on benthic fora-

minifera in the Vienna Basin reflects ecological changes lead-
ing  from  a  “warm  water”  fauna  (lower  Lagenidae  zone)  to  a
“slightly cooler but still warm water” fauna (upper Lagenidae
zone)  (Hohenegger  et  al.  2008).  Thus  the  boundary  between
the lower and upper Lagenidae zones reflects an event in the
climate transition curve. An important biostratigraphic signal
is  the  HCO  of  the  nannoplankton  Helicosphaera  waltrans  at
14.357 ± 0.004 Ma  (Abdul  Aziz  et  al.  2008).

Ar/

Ar sani-

dine dating of a tuff sample from the Styrian Basin contain-
ing H. waltrans (Handler et al. 2006) gave an age of
14.390.12 Ma, confirming that the upper limit of the lower
Lagenidae zone in the Vienna Basin containing H. waltrans
must be younger than, but close to this date (Fig. 3).

HOHENEGGER, ĆORIĆ and WAGREICH

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GEOLOGICA CARPATHICA, 2014, 65, 1, 55—66

Stable oxygen isotopes from the southern ocean show an

initial strong positive excursion between 14.2 and 14.3 Ma in
plankton and benthic foraminifera, as well as a pronounced
δ

C carbon maximum (CM5) at 14.24 Ma (Shevenell et al.

2004).  This  short,  intense  cooling  event  (MSi-1  of  Abreu  &
Haddad 1998) could have been responsible for the global en-
vironmental change around 14.24 Ma, which in the Paratethys
is  seen  in  the  disappearance  of  H.  waltrans  (characterizing
possibly the LO of this species) and the change in the compo-
sition of the benthic foraminiferal fauna from the lower to the
upper  Lagenidae  zone  (Fig. 3).  Strauss  et  al.  (2006)  recog-
nized a sequence boundary in the upper Lagenidae zone (up-
per part according to Rögl et al. 2007b) in the southern Vienna
Basin  on  top  of  their  first  Badenian  cycle.  This  sequence
boundary may be either of a more regional nature (Rögl et al.
2007b)  or  may  be  related  to  a  smaller  sea-level  drop  around
14.2 as recorded by, for example, Kominz et al. (2008).

Furthermore, the base of the tropical plankton Zone M7,

the Fohsella peripheroacuta Lowest-occurrence Zone is also
positioned at 14.24 (Anthonissen & Ogg 2012) or 14.23 Ma
(Wade et al. 2011). The lack of the index fossil F. periphe-
roacuta, characteristic of tropical environments in the upper
Lagenidae zone is in accordance with the slightly cooler wa-
ter during this time interval.

Because the environmental change at 14.24 Ma is seen glo-

bally in the foraminiferal plankton zonation, both Lagenidae
zones restricted to the Vienna Basin can be directly correlated
with  the  tropical  plankton  Zones  M6  and  M7  (Wade  et  al.
2011).  Thus,  we  conclude  that  the  lower  Lagenidae  zone  of
the  Vienna  Basin  corresponds  largely  to  Zone  M6  Orbulina
suturalis Lowest-occurrence Zone from 15.10—14.24/14.23 Ma,
where  the  index  form  is  represented  in  the  Central  Para-
tethys. The subsequent M7 Fohsella peripheroacuta Lowest-
occurrence Zone from 14.24/14.23—13.77/13.74 Ma (Wade et
al. 2011; Anthonissen & Ogg 2012) corresponds in large part
to the upper Lagenidae zone, but so far there is no evidence
for this tropical index fossil in the whole Paratethys. Never-
theless, both zones can be alternatively used to subdivide the
Mid  Badenian  rather  than  the  informal  division  into  lower
and  upper  Lagenidae  zone  that  is  only  valid  for  the  Vienna
Basin (Fig. 3).

Late Badenian

The younger part of the Badenian was subdivided by Papp

et al. (1978a,b) into two substages;  the Wielician (formerly
regarded  as  “middle”  Badenian,  agglutinated  foraminifera
zone) and the Kosovian (“upper” Badenian, Bulimina/Bolivina-
zone  and  the  uppermost  zone  of  impoverished  faunas).  The
timing of these substages is difficult because tectonic uplift
geographically separated the Carpathian Foredeep and Tran-
sylvanian Basin from the Vienna and Pannonian Basins (e.g.
Rögl 1998).

Attribution of the Badenian stratotype from 13.982 to

13.964 Ma (Hohenegger & Wagreich 2012) to the Mid Bad-
enian  as  newly  defined  here  indicates  that  the  age  of  the
Mid/Late  Badenian  boundary  must  be  younger  than
13.964 Ma.  The  next  younger  pronounced  and  dated  global
event thus comprises the Langhian/Serravallian boundary at

13.82 Ma. The GSSP of the Serravallian marks an intense
climatic change, with a strong drop in temperatures (Hilgen
et al. 2009).

Given our dating of the Badenian/Sarmatian boundary at

12.829 Ma,  the  Late  Badenian  extended  from  13.82  to
12.829 Ma, so that it lasted ca. 991 thousand years. The Wieli-
cian  substage  characterized  by  evaporites  within  the  Car-
pathian Foredeep and the Transylvanian Basin (e.g. Peryt et al.
1997; Andreyeva-Grigorovich et al. 2003, 2008; Oszczypko et
al.  2006;  Peryt  2006;  de  Leeuw  et  al.  2010;  Peryt  &  Gedl
2010;  Filipescu  &  de  Leeuw  2011;  de  Leeuw  et  al.  2012)
corresponds to a subunit of the Late Badenian, separating it
from  the  fully  marine  Kosovian  starting  diachronously  from
ca. 13.1  (Śliwiński  et  al.  2012)  to  ca.  13.6 Ma  based  on  sea-
level cycles (Fig. 3, Hardenbol et al. 1998; 13.54 Ma accord-
ing to TS Creator Vers. 6.1, http://www.tscreator.org).

Conclusion

Investigations of the Karpatian and Badenian in the classic

areas of the Austrian Alpine Foredeep and the Styrian Basin
resulted in the detection of a large interval between the up-
permost Karpatian and the base of the lower Lagenidae zone
(the former base of the Badenian), the latter correlated with
the  NN4/NN5  boundary  at  14.91 Ma.  Detailed  integrated
stratigraphical  investigations  in  the  Styrian  Basin  shows  a
clear  paleoenvironmental  change  documented  by  shallow
benthic  foraminifera,  stable  isotopes  and  the  occurrence  of
the  planktonic  foraminifer  Praeorbulina  sicana  together
with  the  marked  change  in  nannofossil  composition  at  ca.
16.3 Ma.  This  change  was  caused  by  a  significant  Alpine
tectonic event named the Styrian Tectonic Phase. On the ba-
sis of this and of magnetostratigraphic correlations, we con-
clude  that  the  base  of  the  Badenian  should  be  placed  at
16.303 Ma and does not coincide with the Burdigalian/Lang-
hian boundary at 15.974 Ma. The interval between 16.303 and
15.032 Ma, named the Early Badenian, corresponds largely to
the 3

order sea-level cycle TB 2.3 (Haq et al. 1988).

The lower Lagenidae zone of the newly defined Mid Bade-

nian belonging to the NN5 Zone starts at 15.032 Ma, which
is  the  top  of  polarity  Chron  C5Bn.2n,  and  is  terminated  at
14.24 Ma due to the short cooling event in the Middle Mio-
cene  climate  transition  curve  (Fig. 3).  The  stratotype  of  the
Badenian  stage  in  the  southern  Vienna  Basin,  belonging  to
the  upper  Lagenidae  zone,  has  recently  been  calibrated  by
cross-correlating  geophysical  and  geochemical  variables
with  the  mid-summer  insolation  curve  (Hohenegger  &
Wagreich  2012).  This  resulted  in  an  age  between  —13.982
( + 0.003/—0.002)  Ma  and  —13.964  ( + 0.003/—0.002) Ma  for
the stratotype section.

The significant

O increase at 13.82 Ma, determined as

the Langhian/Serravallian boundary, can be linked with the
end of the Mid Badenian and beginning of the Late Bade-
nian. The Badenian/Sarmatian boundary, possibly reflecting
a sequence boundary finishing cycle TB 2.5 is placed at the
top of polarity Chron C5Ar2n at 12.829 Ma.

The new chronometric division into an Early, Mid and

Late Badenian correlates with the global 3

order sequences

TIMING OF THE REGIONAL BADENIAN STAGE (MIDDLE MIOCENE, CENTRAL PARATETHYS)

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GEOLOGICA CARPATHICA, 2014, 65, 1, 55—66

TB 2.3, TB 2.4 and particularly well with TB 2.5, with dura-
tions that are in the order of 1 million years each. The bound-
aries between these ages are either magnetostratigraphically
or  climatically,  and  thus  astronomically,  fixed,  with  good
support from biostratigraphic markers. The informal division
of  the  Badenian  into  the  lower  and  upper  Lagenidae  Zone,
the Spiroplectammina Zone and the Bulimina/Bolivina Zone,
restricted to the Vienna Basin, can be correlated to the global
plankton Praeorbulina sicana Zone marking the Early Bade-
nian,  Orbulina  suturalis  and  Fohsella  peripheroacuta  Zone
marking the Mid Badenian, and Velapertina indigena mark-
ing the Late Badenian in the Central Paratethys.

Finally, the new subdivision of the Badenian correlates

with  the  paleoclimatic  evolution  of  the  Middle  Miocene,
where the Early Badenian approximately corresponds to the
“Middle Miocene Climate Optimum”. The Mid Badenian is
characterized  by  the  “Middle  Miocene  Climate  Transition”
and the Late Badenian is governed by the initial part of the
“Middle  Miocene  Icehouse”  reflecting  the  restarting  of
Antarctic glaciation.

The proposed new chronometric timing of the Badenian

makes  reconsideration  of  the  chronostratigraphic  substages
necessary, because the holostratotypes of all substages do not
contain  the  basal  boundaries  (Papp  et  al.  1978a).  The  basal
Moravian spanning both the Early and Mid Badenian in time
should be restricted to the latter by redefinition based on a new
boundary stratotype, while the Early Badenian becomes open
for the definition of a new substage necessarily determined by
a boundary stratotype. The Wagna section (Fig. 2) cannot be
used  as  a  boundary  stratotype  because  it  lacks  a  continuous
transition from the Karpatian into the Badenian. Redefinition
and  chronometric  timing  of  the  Late  Badenian  substages
Wielician  and  Kosovian  is  also  essential  for  establishing
boundary stratotypes based on isochronous events.

Acknowledgments:  This  paper  is  based  on  results  of  the
FWF Projects P13743-BIO, P13740-GEO, P16793-B06 and
P13738-Tec of the Austrian Science Fund. We thank all co-
workers  within  these  projects  in  alphabetical  order:  Katalin
Bàldi,  Maksuda  Khatun,  Peter  Pervesler,  Reinhard  Roetzel,
Christian  Rupp,  Robert  Scholger,  Anna  Selge,  Silvia  Spez-
zaferri  und  Karl  Stingl.  Special  thanks  are  due  to  the  Fred
Rögl  for  corrections  and  giving  important  comments.  Sorin
Filipescu,  Marta  Oszczypko-Clowes  and  Lilian  Švábenická
together  with  an  anonymous  reviewer  helped  in  clarifying
problems. Hugh Rice improved and corrected the text.

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