GeolCarp_Vol59_No6_545

GEOLOGICA CARPATHICA, DECEMBER 2008, 59, 6, 545—561

www.geologicacarpathica.sk

Serravallian sequence stratigraphy of the northern

Vienna Basin: high frequency cycles in the Sarmatian

sedimentary record

MICHAL KOVÁČ, UBOMÍR SLIVA, BOHUSLAVA SOPKOVÁ, JANA HLAVATÁ

and ADRIANA ŠKULOVÁ

Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G, 842 15 Bratislava,

Slovak Republic; kovacm@fns.uniba.sk

(Manuscript received November 5, 2007; accepted in revised form June 12, 2008)

Abstract: Middle Miocene global and regional factors affecting the development of depositional systems and sedimentary
architecture were studied in the northern Vienna Basin. In the Serravallian sedimentary record (Upper Badenian and
Sarmatian, Central Paratethys regional stages) two individual 3

-order cycles of sea-level changes were confirmed. They

can be more or less compared with Haq’s Mediterranean cycles TB 2.5 and TB 2.6. The presented sequence stratigraphy
approach also proved existence of four 4

-order relative sea-level changes in this time interval here. Furthermore, the late

Serravallian (Sarmatian) record documents the strong influence of astronomical forcing on cyclic sedimentation. Detected
high frequency cycles are most likely result of climatic (orbital) forcing on the eccentricity band with period of 400 and
100 kyr in a shallow water depositional environment. The sequence stratigraphy scheme of the northern Vienna Basin fits
well with development in the whole basin, as well as with development in other basins in the Carpathian-Pannonian region
(Styrian and Transylvanian Basins). This fact therefore led to the assumption of an interregional character of the high
frequency cycles initiated by impulses common for different basins in the Central Paratethys realm.

Key words: Sarmatian, Upper Badenian, Vienna Basin, sequence stratigraphy, depositional systems, cyclic sedimentation,
high frequency cycles.

Introduction

Study of the sedimentary record in the northern Vienna Ba-
sin (Slovak part) was focused on the Serravallian basin fill
architecture, determination of the depositional environments
and cyclicity of the sedimentary record. The research traces
the occurrence of global events in the Vienna Basin (e.g. glo-
bal 3

-order sea-level changes) known from the whole Cen-

tral Paratethys domain (Vakarcs et al. 1994, 1998; Pavelić et
al.  1998;  Kováč  et  al.  2001,  2007;  Krézsek  &  Filipescu
2005;  Strauss  et  al.  2006;  Piller  et  al.  2007),  as  well  as  re-
gional  events  (e.g.  4

-order cycles of relative sea-level

changes). Special emphasis was given to detailed study of
high frequency cycles as a result of interactions between cli-
matic influence and the dynamics of shallow water sedimen-
tary environments during the late Serravallian (Sarmatian).

Geological setting and outline of the Vienna Basin’s

paleogeography

The Vienna Basin, situated in the Alpine-Carpathian junc-

tion, covers parts of three states. Its north-western part ex-
tends into the Czech Republic, the southern part,
representing more than 50% of the basin is situated in Aus-
tria, whereas its north-eastern part lies in Slovakia (Fig. 1).

The Vienna Basin was described as a typical pull-apart ba-

sin (Royden 1985; Fodor 1995), nevertheless the tectonic

history also documents an Early Miocene evolutionary stage
of piggy-back basins and wrench fault furrows and a Middle
to  Late  Miocene  extensional  basin  development  of  graben
and  horst  structures  (Kováč  2000;  Kováč  et  al.  2004).  The
basin  is  superimposed  on  tectonic  units  of  the  Flysch  Zone
(Rhenodanubian  Flysch  and  Outer  Western  Carpathians)  in
the West and North. The pre-Neogene basement in the south-
ern, central and eastern part is built up by units of the North-
ern  Calcareous  Alps,  Central  Eastern  Alps  and  Central
Western  Carpathians  (Fig. 1).  Neogene  sedimentary  fill
reaches  a  thickness  of  up  to  5500 m  in  the  basin’s  deepest
part (Kilenyi & Šefara 1989).

The basin pull-apart depocentres developed at the end of

the Early Miocene during the initial rifting stage, which was
associated with the extrusion of the Western Carpathians
from the East Alpine domain (Ratschbacher et al. 1991a,b).
The Middle Miocene basin evolution was overtaken by re-
gional extensional tectonics. The subsidence of the basin de-
pocentres was controlled predominantly by the NE-SW and
NNE-SSW oriented normal faults. Grabens, halfgrabens and
elevations were formed (Lankreijer et al. 1995).

The Serravalian (Late Badenian and Sarmatian) structural

development  of  the  basin,  as  well  as  the  development  of
neighbouring mountain ranges, induced important changes in
the  river  drainage  system,  transport  of  sediments  and  forma-
tion of deltaic systems (Fig. 2). The older, Early Miocene del-
ta entering the basin from the south (Aderklaa Formation) was
replaced  by  the  large  Middle  Miocene  deltaic  bodies  on  the

546

KOVÁČ, SLIVA, SOPKOVÁ, HLAVATÁ and ŠKULOVÁ

western (paleo-Danube river delta) and northern margin of the
basin (paleo-Morava river delta). The basin accommodation
space was continuously filled up due to intense sediment sup-
ply in this time (Jiříček & Seifert 1990; Jiříček 2002).

The Middle Miocene Vienna Basin, with respect to paleo-

geographical setting, can be regarded as a semi-closed basin,
an embayment of the Central Paratethys Sea surrounded by
the Alpine-Carpathian-Dinaride mountain chains. The basin,
situated on the north-western margin of the Pannonian Basin
System (Rögl 1998; Kováč et al. 2004, 2007) was connected
with  remaining  epicontinental  sea  only  through  the  Eisen-
stadt  Basin  and  Ödenburg  Gate  in  the  SE,  further  by  the
Devín-Hainburg and by the Jablonica Gates in the E and NE
(Fig. 2).  In  spite  of  this,  the  global  and  regional  sea-level
changes  traceable  in  the  Vienna  Basin  are  similar  to  the
changes in the Pannonian Basin System, covered by the Cen-
tral  Paratethys  Sea  during  this  time  (Harzhauser  &  Piller
2007; Kováč et al. 2007).

The connection of the Central Paratethys Sea with the

Mediterranean – via Trans-Tethydian Trench Corridor had
already been closed before the Serravallian (in Middle Bade-
nian). Other, disputable sea connections had disappeared
during the early Serravallian (in Late Badenian, Rögl 1998;

Harzhauser & Piller 2007; Kováč et al. 2007). The late Ser-
ravallian  (Sarmatian)  sedimentary  environment  of  the  Cen-
tral Paratethys already has signs of strong isolation from the
open sea areas, which are documented by the specific com-
position  of  brine  (Pisera  1996)  and  endemic  faunas
(Harzhauser & Piller 2007). From the climatic point of view,
the  Middle  Miocene  Climatic  Optimum  ended  here  in  the
early  Serravallian  (Late  Badenian,  Böhme  2003)  and  in  the
late Serravallian (Sarmatian) a shift towards a Mediterranean
temperate  climate  was  documented  (Kvaček  et  al.  2006;
Harzhauser et al. 2007).

Methods

The presented research was supported by study of archive

materials of the Oil and Gas Exploration Company NAFTA,
comprising 89 Final reports for individual wells, including
well logs for each well (Spontaneous Potential – SP, Resis-
tivity log – RAG; and a limited number of Gamma logs –
GKA), seismic profiles and available borehole cores.

The field methods included sedimentological study of

borehole  cores  combined  with  sampling  for  micropaleonto-
logical  high-resolution  analysis.  Well  logs  of  all  boreholes
were  compared  and  processed  under  principles  of  electro-se-
quence analysis (Van Wagoner et al. 1990; Rider 1996; Emery
& Myers 1996; Catuneanu 2002). The well logs were used to
determine general trends of individual parasequences to ob-
tain  a  general  trend  for  the  whole  sedimentary  record.  For
comparison, migrated seismic lines were used, to check well
log motifs with their responses on the seismic profiles. The
acquired data were further confronted with the results of sed-
imentological and micropaleontological analysis of cores, to
provide reliable final information (Kováč et al. 2001, 2005,
2008;  Fordinál  et  al.  2002,  2003,  2006;  Bartakovics  &
Hudáčková 2004; Kováčová et al. 2008).

Time scale

The studied time span covers the Mediterranean stage –

the Serravallian, with its duration from 13.65 ± 0.05 to
11.608 ± 0.005 Ma, assigned to the Middle Miocene sub-ep-
och (Gradstein et al. 2004). In the regional Central Para-
tethys time scale the Serravallian is considered to be the Late
Badenian and Sarmatian stage (Table 1).

The Late Badenian stage of the Central Paratethys span-

ning from 13.65 Ma to 12.7 Ma corresponds to the early Ser-
ravallian of the Mediterranean, as well as to the Konkian
regional stage of the Eastern Paratethys (Papp et al. 1978;
Gradstein et al. 2004; Kováč et al. 2007).

The Sarmatian stage covers a time span of 12.7—11.6 Ma

and corresponds to the late Serravallian of the Mediterranean
and to the Volhynian and early Bessarabian stages of the East-
ern Paratethys (Papp et al. 1974; Gradstein et al. 2004). Ac-
cording to Abreu & Haddad (1998), the lower boundary of the
Sarmatian fits very well with the glacio-eustatic isotope event
MSI-3 at 12.7 Ma and its upper boundary corresponds to the
glacio-eustatic sea-level lowstand of cycle TB 3.1 at 11.6 Ma,

Fig. 1. Simplified geological map of the Vienna Basin, situated at
the East Alpine—Western Carpathian junction (modified after Lexa
et al. 2000).

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SERRAVALLIAN SEQUENCE STRATIGRAPHY OF THE VIENNA BASIN: HIGH FREQUENCY CYCLES

although no absolute dating of these boundaries is available
up to now (Harzhauser & Piller 2004).

Chrono- and biostratigraphy

The base of the Serravallian was defined by the last occur-

rence (LO) of the nannofossil Sphenolithus heteromorphus
within the magnetic polarity Chronozone C5ABr. The end is
characterized by the last common occurrence of the calcareous
nannofossil Discoaster kugleri and the planktonic foraminifer
Globigerinoides subquadratus. Assosiated with the short nor-
mal polarity Subchron C5r.2n (Gradstein et al. 2004).

The base of the Late Badenian was defined by the onset

of the planktonic foraminiferal Velapertina indigena Zone as
well as by the extinction of the Sphenolithus heteromorphus,
referring to the NN5c Zone and the first occurrence of Dis-
coaster exilis that falls within the calcareous nannoplankton

NN6  Zone  (Andrejeva-Grigor-
ovich  et  al.  2001).  Further,  ac-
cording to Grill (1941, 1943) the
Late  Badenian  can  be  character-
ized  by  foraminiferal  associa-
tions  of  the  Bolimina/Bulivina
Zone,  whereas  in  marginal  parts
of  the  basin  depleted  brackish
Ammonia  beccarii  associations
often prevails.

The previous three-fold biozo-

nation  of  the  Sarmatian  stage
(according Grill 1941, 1943) us-
ing the foraminiferal assemblag-
es:  Elphidium  reginum  Zone,
Elphidium  hauerinum  Zone  and
Nonion

granosum

( = Po-

rosononion)  Zone  has  recently
been revised into a two-fold divi-
sion (Table 1); the Early Sarma-
tian  comprising  foraminiferal
Anomalinoides dividens,  Elphidi-
um  reginum  and  Elphidium
hauerinum  Zones  and  the  Late
Sarmatian  containing  the  Po-
rosononion

granosum

Zone

(Harzhauser  &  Piller  2004).  Be-
side  the  zonation  based  on  fora-
minifera,  molluscs  also  provide
reliable  biostratigraphic  markers.
The  Early  Sarmatian  spans  the
Mohrensternia Zone and the low-
er part of the Ervilia Zone and the
Late Sarmatian comprises the up-
per  part  of  the  Ervilia  Zone  and
the

Sarmatimactra

vitaliana

Zone  of  Harzhauser  &  Piller
(2004).  Jiříček  (1970,  1972)  di-
vided  the  Sarmatian  according
ostracodes  into  the  Early  Sarma-
tian with A—B Zones represented

Fig. 2. Paleogeographical development of the Vienna Basin from Lower to Middle Miocene docu-
menting change in the position and development of prograding delta bodies entering the basin
(modified after Kováč 2000).

by Aurila mehesi and the Late Sarmatian with the C—E Zones
with occurrence of Aurila notata (Jiříček 2002).

Sedimentary record

The Upper Badenian sediments are represented by the

Studienka Formation in the Slovak part of the Vienna Ba-
sin  (Table 1).  The  offshore  facies  consist  mostly  of  fine-
grained greenish-grey calcareous clays/claystones reaching a
thickness of up to 400—600 m (Špička 1969). The Bulimina-
Bolivina  Zone  foraminiferal  associations  indicate  stratifica-
tion  of  the  water  column  with  low  oxygen  content  near  the
basin bottom (Hudáčková & Kováč 1993). Towards the ba-
sin  margins  the  marine  calcareous  clays  (“marls”)  and  silt-
stones  are  replaced  by  more  sandy  onshore  facies.  In  the
uppermost part of the sequence dark clays with coal beds oc-
cur in some places.

548

KOVÁČ, SLIVA, SOPKOVÁ, HLAVATÁ and ŠKULOVÁ

The shallow water sedimentation at the basin margin is

represented by the transgressive Sandberg Member to the
East and the deltaic Gajary Member to the West (Table 1).

The Sandberg Member (Baráth et al. 1994) lies discor-

dantly on the underlying pre-Neogene basement and is
formed mainly by cross-bedded yellow-grey sand with inter-
calation of gravel and sandy-clays layers. Algal biostromes
occur as well. The thickness of the deposits does not exceed
100 m.

The Gajary Member (Vass 1989) consists mainly of

sandy sediments interbedded with calcareous clays and silts,
reaching a thickness of about 100 m. The member is espe-
cially distributed along the Slovak-Austrian boundary and
refers to a large delta entering the basin from the West.

The Upper Badenian sediments in the study area, in the

north-eastern  offshore  zone  of  the  Vienna  Basin,  belong  to
Studienka  Formation.  The  cores  (Table 3)  are  composed
mainly of grey calcareous clays/claystones, often bioturbat-
ed,  containing  molluscs  fragments  (Fordinál  et  al.  2002,
2003;  Bartakovics  &  Hudáčková  2004;  Kováč  et  al.  2008).
Towards the overlying strata calcareous clays pass into sands
and  silts  deposited  in  a  shallow,  brackish  environment  (Ta-
ble 3). In the western part of study area, the clays are locally
substituted by deltaic sands of the Gajary Member (Kováč et
al. 2005, 2008).

The Sarmatian sediments of the Vienna Basin can be sub-

divided into two parts – the Holíč and Skalica Formations
(Tables 1, 2).

The Lower Sarmatian, Holíč Formation is represented by

grey calcareous clay, silt and rare acidic tuff layers (Vass
2002). According to Elečko & Vass (2001) fluvial gravels
representing the Radimov Member in the northern tip of the

basin  and  the  Kopčany  Member,  consisting  of  variegated
and spotted pelites with scattered lenses of sand represent the
lowermost Sarmatian deposits in the northern part of the Vien-
na  Basin,  in  the  Kúty  and  Kopčany  grabens.  The  Kopčany
Member has also been known as the Carychium beds (Jiříček
1973). The next informal lithostratigraphic term the “Beds of
Hölles” was introduced by Brix & Plöchinger (1988) within
the central and southern part of the basin, composed mainly
of coarse-grained sediments on the margins, whereas in basi-
nal  settings  predominantly  marls  with  coarse  intercalations
are present. In marginal settings bryzoan-serpulid-algae bio-
constructions  and  several  meters  thick  pale  limestones  are
situated (Harzhauser & Piller 2004).

The Upper Sarmatian Skalica Formation displays various

lithologies, ranging from marl and silt to sandstone and grav-
el  with  various  siliciclastic  and  carbonatic  deposits  such  as
oolites,  rock-forming  coquinas  and  foraminiferal  biocon-
structions (Elečko & Vass 2001; Vass 2002). The Wolfsthal
Member  is  wide-spread  along  margins  of  the  basin  and  in-
cludes the rock-forming oolitic coquinas (Harzhauser & Pill-
er 2004). In basinal settings, carbonate facies are replaced by
fossiliferous sandy to clayey marls, which have been named
in  the  central  and  southern  Vienna  Basin  as  the  “Beds  of
Kottingbrung” by Brix & Plöchinger (1988).

Sarmatian strata in the study area comprise predominantly

grey clays and silts along with sands of the Lower Sarmatian
Holíč  Formation  (Table 3).  In  cores  foraminiferal  assem-
blages of Anomalinoides dividens Zone, Elphidium reginum
Zone and Elphidium hauerinum Zone were detected (Kováč
et  al.  2005,  2008).  Upwards,  the  Skalica  Formation  repre-
sents  the  Upper  Sarmatian  fill,  built  up  by  clays,  silts  and
sandstone layers (Table 3) with occurrences of foraminiferal

Table 1: Chronostratigraphy and biostratigraphy of the Serravallian (Late Badenian and Sarmatian) sediments of the Vienna Basin: calcar-
eous nannoplankton (Martini 1971; Raffi et al. 2003), foraminifera (Grill 1941, 1943), molluscs (Harzhauser & Piller 2004); litostratigra-
phy (Vass 2002); Mediteranean sea-level changes (sensu Haq et al. 1988 and Hardenbol et al. 1998, modified after Gradstein et al. 2004.)

549

SERRAVALLIAN SEQUENCE STRATIGRAPHY OF THE VIENNA BASIN: HIGH FREQUENCY CYCLES

assemblages of the Porosononion granosum Zone (Kováč et
al. 2005, 2008; Fordinál et al. 2006).

Depositional environment

The Upper Badenian sedimentary record in the study

area, in the north-eastern part of Vienna Basin (Fig. 1) shows
a gradual transition from the offshore environment to the en-
vironment  of  a  distal  delta  setting  (prodelta).  Toward  the
overlying  strata  the  depositional  environment  became  shal-
lower  and  shallower.  The  foraminiferal  associations  of  the
Bulimina-Bolivina  Zone  are  replaced  here  by  assemblages
with  prevalence  of  Ammonia  beccarii  (Kováč  et  al.  2005,
2008). Shoaling was caused by the eastward progradation of
delta lobes (Figs. 3, 4). Increased sediment supply also led to
the onset of forced regression. Summarizing the evolution of
the  depositional  environment  in  the  Upper  Badenian  se-
quence within the studied area, the following changes could
be  established:  offshore—prodelta—delta  slope—delta  front
with prograding mouth bars – delta plain with distributary
and  interdistributary  areas  displaying  common  distributary
channel  avulsion  (based  on  detailed  descriptions  of  seismic
lines  (Figs. 3,  4),  well  logs  (Fig. 5)  and  cores  (Table 3)
which follow in the next part of this paper, dealing with se-
quence stratigraphy).

The Sarmatian sedimentary record reveals deposition in a

shallow  marine,  near  shore  deltaic  environment.  The  Lower
Sarmatian  sedimentation  starts  with  a  muddy  sequence,  de-
posited in a relatively quiet environment of the distal area of
deltaic  lobes.  Towards  the  overlying  strata,  transition  from
clays to sandy clays and silts is documented (Fig. 5) and it is
interpreted as a continual change from basinal environment to
the environment of delta plain (Table 3). In the middle part of
the  sedimentary  column  increased  input  of  clastic  material
was observed, which can be connected with regional tectonics
inducing paleogeographical changes of depocentres as well as
shift of the deltaic lobes (Kováč et al. 2004, 2008). The sedi-
ments in the uppermost part of sequence, containing common
plant  detritus,  were  deposited  in  an  environment  of  shallow
marshes  or  hyposaline  lagoons,  frequently  foraminiferal  as-
semblages with Ammonia beccarii (Linné) were found (Kováč
et al. 2008). Study of borehole cores point to the environment
of muddy tidal flats. The silts and sands often comprise flaser
and  lenticular  beddings;  thus,  we  suppose  deposition  mainly
in the subtidal to intertidal zone (Table 3).

Study of cores and well logs enabled consideration, that

the sedimentary environment on the north-eastern margin of
the Vienna Basin was composed of distributary channels and
interdistributary areas, represented by swamp and marsh sys-
tems  (Table 3,  Figs. 5,  6).  Distributaries  are  designated  by
the number of leveed channels, passing basinward to mouth
bars, yielding clastic material derived from NW—N. Evident
fluctuations  recorded  between  the  stacked  parasequences  in
well  logs  can  be  related  to  the  distributary  channels/mouth
bars shifts (Fig. 5). Upwards, we suggest increased sediment
load to be reworked by coastal currents in the form of indi-
vidual,  laterally  extensive  sand  bodies,  distinguishable  in
well  logs  (Fig. 6).  According  to  the  sedimentological  and

micropaleontological  study  of  borehole  cores  (Kováč  et  al.
2008), a gradual shift was recorded from a subtidal to an in-
tertidal environment, ranging from the tidal flats to vegetated
marshes.  Micropaleontological  study  (occurrence  of  miliol-
ids association) and rich plant detritus also points to the very
shallow water environment of the intermediate, hyper or hy-
posaline marshes overgrown by vegetation (Tables 2, 3). The
character  of  marsh  and  very  shallow  water  sedimentation
continued till the end of the Early Sarmatian.

The onset of the Upper Sarmatian environment, interpret-

ed  from  cores  and  well  logs,  can  be  characterized  by  the
presence of sand ridges and sandy bodies reworked by coast-
al  currents  and  occasionally  by  shallow  incised  tidal  chan-
nels  on  the  coastal  plain  (Table 3,  Figs. 5,  6).  The  clastic
material transported by along-shore coastal currents, formed
some kind of barriers triggering the sedimentation in protect-
ed  bays  or  lagoons.  Furthermore,  continual  shallowing  up-
ward  was  accompanied  by  the  onset  of  the  foraminiferal
assemblages  with  Porosonion  granosum  (d’Orbigny)
monoassociations,  typical  for  the  brackish  shallow  environ-
ment (Fordinál et al. 2006; Kováč et al. 2008). The environ-
ment of marshes was recorded in cores by occurrence of seed
remnants  of  the  Glyptostrobus  europaeus  (Brongniart).  At
the end of the Late Sarmatian even deposition of lignite lay-
ers within the coastal flats was proved.

Seismic profiles

On the interpreted NWW-SEE oriented seismic profiles in

the  northern  Vienna  Basin  (Fig. 1)  distinct  basinward  pro-
grading  clinoform  bodies  belonging  to  the  Badenian  record
(Figs. 3,  4)  can  be  recognized.  The  lower  clinoform  is  as-
signed to the Middle Badenian; the upper clinoform was de-
posited  during  the  Late  Badenian  sub-stage.  Recognition  of
delta topsets, foresets and bottomsets is based on the config-
uration of reflections.

The lower wedge-shaped body reflectors downlap onto

more  or  less  horizontal  reflections  of  underlying  strata,
which  refer  to  the  maximum  flooding  surface  (mfs)  in  the
sedimentary  record  of  the  Middle  Badenian.  The  upper
boundary  of  the  clinoform  represents  a  sequence  boundary
of type 2 (SB 2). Onlapping reflexes onto the foreset of the
Middle  Badenian  clinoform  body  most  likely  indicate  the
Late Badenian transgression.

The overlying Upper Badenian clinoform is characterized

by a sigmoidal configuration of seismic responses, which
pass eastward into flat laying parallel responses referring to a
prodelta sedimentary environment. The sigmoidal configura-
tion of seismic reflexes points to quiet, undisturbed deposi-
tional conditions with continuous sediment supply (sensu
Mitchum 1977; Vail et al. 1977; Miall 2000).

Furthermore, in the very eastern part of some seismic sec-

tions  a  third  sedimentary  body  was  identified  (Fig. 3).  This
body  shows  strong  (sharp)  seismical  responses,  what  can  be
related to sedimentation of coarser material. These seismic re-
flections  show  a  typical  onlap  pattern,  what  is  presumably
caused  by  the  subsequent  compaction,  and  therefore  –  be-
cause of their uncertain original position – such sedimentary
package  could  represent  fluvial  lowstand  deposits  of  the  fol-

550

KOVÁČ, SLIVA, SOPKOVÁ, HLAVATÁ and ŠKULOVÁ

lowing  cycle  of  relative  sea-level  change  (sensu  Catuneanu
2002). A lowstand system tract (LST), with fluvial character
of  sedimentation,  defined  by  strong  seismic  responses  was
also  confirmed  on  well  logs  by  typical  prograding  funnel-
shaped  pattern,  related  to  the  deposition  in  mouth-bars
(Fig. 5). Even though the sediments are dated by biostratigra-
phy as Late Badenian (Fordinál et al. 2002, 2003; Kováč et al.
2008) they are associated with the sedimentary architecture of
the next Sarmatian cycle of relative sea-level change. Conse-
quently,  we  propose  to  interpret  this  boundary  as  SB 2/SB 1
at the base of following cycle (Fig. 3). The observed phenom-
enon – e.g. beginning of the “Sarmatian cycle in terminology
of  the  Sequence  stratigraphy”  already  during  the  termination
of the “Late Badenian in terminology of the Biostratigraphy”
– is comparable to a similar development of the Late Bade-
nian and Sarmatian 3

-order cycles in the Transylvanian Ba-

sin (sensu Krészek & Filipescu 2005).

Other seismic profiles from

the  studied  area  reveal  differ-
ent  configurations  of  seismic
responses.  On  these  profiles
the  above  mentioned  low-
stand deposits (LST) are miss-
ing  (Fig. 4).  The  presence  of
an  erosional  unconformity
was  documented  on  the  basis
of  toplap  termination  of  the
Late  Badenian  reflexes.  The
identified  erosional  surface  is
also  well  observable  on  the
well  logs  as  a  new  onset  of
channel  fill  sands  (Fig. 5).
This datum most likely repre-
sents  an  erosional  surface,
which  originated  after  a  con-
siderable sea-level drop at the
turn of the Late Badenian and
Sarmatian.  The  identified  un-
conformity is assigned to a se-
quence  boundary  of  type 1
(SB 1),  which  continuously
passes  eastward  into  a  se-
quence  boundary  of  type 2
(SB 2).  The  explanation  of
this  fact  is  that  the  Upper
Badenian  highstand  deltaic
sediments  underwent  erosion
before  they  were  overlain
(covered)  by  the  Sarmatian
deposits.  The  onset  of  the
next  sequence  is  marked  not
only  by  an  erosive  discor-
dance, but also by partly cha-
otic  reflectors  with  downlaps
in  the  western  part  of  some
seismic profiles (Fig. 3).

From the lithological point

of view the Badenian clino-
form bodies on the eastern

Fig. 3. Interpreted seismic profile of the Badenian and Sarmatian (Serravallian) sedimentary record
(profile location see Fig. 1). Notice the Sarmatian fluvial lowstand deposits (LST) in the eastern sec-
tion of the seismic profile.

margin of the Vienna Basin are composed mainly of pelitic
material. Clays prevail particularly in the depositional envi-
roment  of  topsets  and  bottomsets.  The  area  of  deltaic  fore-
sets  shows  a  sharpening  of  seismic  responses,  which  could
indicate  increased  sedimentation  of  coarser  material  (sands
and silts) referring to the presence of mouth bars.

The Sarmatian sediments are marked by an absence of dis-

tinct clinoforms caused by shallow accomodation space of the
Sarmatian sea in the studied area (Fig. 1). These deposits are
recorded by relatively subhorizontal to horizontal seismic re-
flectors,  which  point  to  the  trends  of  high  frequency  cycles,
represented  by  planar  sand  bodies  alternating  with  fine-
grained clays and silts (Figs. 3, 4). The distribution and bed-
ding  of  sediments  indicates  slight  differences  within  the
Lower and Upper Sarmatian strata.

When tracing seismic responses as well as the well log mo-

tifs, it is possible to observe that the bio- and sequence stratig-

551

SERRAVALLIAN SEQUENCE STRATIGRAPHY OF THE VIENNA BASIN: HIGH FREQUENCY CYCLES

Fig. 4. Interpreted seismic profile of the Badenian and Sarmatian (Serravallian) sedimentary record
(profile location see Fig. 1). Notice the distinct erosional surface on the Late Badenian/Sarmatian
boundary.

raphy  boundaries  do  not match  exactly. The  explanation  of
this fact is easy. In our case, it is generally accepted, that at the
Badenian/Sarmatian  boundary  there  was  a  considerable  sea-
level drop, what is recognized as a SB 1 (Kováč et al. 2004;
Strauss et al. 2006). Erosion and transport of the Upper Bade-
nian sediments is associated with the redeposition and enrich-
ment  of  the  deposits  by  the  Late  Badenian  foraminiferal
associations. Therefore, their following deposition during the
Sarmatian LST of the 3

-order cycle apparently started at the

termination of the “Late Badenian” and the Early Sarmatian
transgression can be clearly documented first of all by bios-
tratigraphy.

The same is considered for the Sarmatian/Pannonian

boundary, where the Pannonian cycle also seems to start at
the end of the Sarmatian stage deposition, which is shown by
the easily identifiable transgressive surface (Figs. 3, 4).

Sequence stratigraphy

The sequence stratigraphy framework was applied for the

first time within the area of the northern part of the Vienna Ba-
sin in the 90’s (Kováč et al. 1998). The studies represent an at-
tempt to resolve the influence of relative sea-level changes on

sedimentation  and  paleoenvi-
ronment as well as their influ-
ence  on  the  sedimentary
record of the basin. The mutu-
al  interplay  between  global
sea-level  changes,  tectonics
and sediment supply were tak-
en  into  account  as  well.  The
following  works  of  Kováč  et
al.  (2001,  2004),  Harzhauser
&  Piller  (2004),  Strauss  et  al.
(2006)  have  recognized  in  the
Miocene  sedimentary  fill  of
the basin nine 3

-order cycles,

composing the sedimentary ar-
chitecture.  From  those  cycles,
one  individual  cycle  of  rela-
tive  sea-level  change  belongs
to  the  Late  Badenian  and  one
cycle represents the Sarmatian
sedimentary record.

Third-order cycles of relative
sea-level changes in the sedi-
mentary record of the north-
ern Vienna Basin

In the Vienna Basin, the

Late Badenian sedimentation
represents an individual 3

order cycle of relative sea-
level

change,

that

comparable to the TB 2.5 cy-
cle according to Haq et al.
(1988) or it corresponds to the

time  span  between  the  sequence  boundaries  Ser-2
(13.65 Ma)  and  Ser-3  (12.7 Ma)  identified  by  Hardenbol  et
al.  (1998).  The  Sarmatian,  spanning  the  time  interval  from
12.7 to 11.61 Ma, also comprises in the Vienna Basin a sin-
gle 3

-order cycle, which is comparable to the TB 2.6 cycle

of relative sea-level changes according Haq et al. (1988) and
the Ser-3 (base) and Ser-4/Tor-1 (top) boundaries of Harden-
bol et al. (1998).

In general, the Late Badenian 3

-order cycle starts after a

relative sea-level drop in the Vienna Basin (Kováč et al. 2004;
Strauss et al. 2006). The most representative evidence of the
following transgression is the Sandberg Member on the east-
ern margin of the Vienna Basin (Baráth et al. 1994; Holec &
Sabol 1996). Here the Upper Badenian strata directly overlie
the pre-Neogene basement of the Western Carpathians, repre-
senting  a  distinct  unconformity  (SB 1).  In  the  central  part  of
the  basin  the  sedimentation  continued  without  apparent  evi-
dence of subaerial erosion. Thus, for the eastern offshore zone
of  the  basin,  a  conformable  sequence  boundary  of  type 2
(SB 2) was proposed (Kováč et al. 2004).

The Late Badenian sedimentation was strongly influenced

by a deltaic system, entering the basin from its western margin
since the Early-Middle Badenian (Jiříček & Seifert 1990).
This large delta belonging to the paleo-Danube river (in oil

553

SERRAVALLIAN SEQUENCE STRATIGRAPHY OF THE VIENNA BASIN: HIGH FREQUENCY CYCLES

coarser  material  (silts,  sands)  supplied  from  the  West.  The
transgressive systems tract (TST) could generally be identi-
fied  on  the  basis  of  retrogradational  parasequence  stacking
pattern trend on well logs (Fig. 5), that refers to gradual deep-
ening of the depositional environment. In the studied area the
TST  is  formed  mainly  by  delta  front  sandy  mouth  bars.  The
highstand  system  tract  (HST)  is  characterized  by  the  east-
ward  progradation  of  deltaic  clinoforms  as  a  result  of  forced
regression (Figs. 3, 4). These progradational clinoforms show
sigmoidal seismic responses on the seismic sections. They re-
fer to sedimentation in the lower delta plain environment, with
common channel avulsion and alternation of distributary and
interdistributary depositional settings.

The Sarmatian 3

-order cycle of relative sea-level chang-

es is restricted by the lower boundary of SB type 1 or SB
type 2 (Harzhauser & Piller 2004; Kováč et al. 2004; Straus et
al. 2006). The erosional unconformity (SB 1) has been regis-
tered only in the north-western part of the study area. It is doc-

on well logs, the sands were deposited in flat channels, mouth
bars and sand waves (Fig. 6). The top of the Sarmatian strata
is bounded by the SB 2 or SB 1. The “Sarmatian/Pannonian”
cycles transition in the sense of sequence stratigraphy, repre-
sented by distinct erosional unconformity of SB type 1, is fre-
quently located in the lower Pannonian sedimentary record,
between the B—C Zones (sensu Papp 1951; Kováč et al. 1998).

Fourth-order cycles of relative sea-level changes in the
sedimentary record of the northern Vienna Basin

The 4

-order cycles of relative sea-level change mirror re-

gional or local impulses, which affected the sedimentary record
(climate, sediment supply, local tectonics). Nevertheless, the
changes of depositional environment in the sedimentary record
of the Vienna Basin can be traced and even correlated with oth-
er basins of the Central Paratethys (see Kováč et al. 2001, 2007;
Harzhauser & Piller 2004, 2007; Krészek & Filipescu 2005)

Table 2: 3

- and 4

-order cycles of relative sea-level changes, well log record refer-

ring to changes in depositional environment (borehole M1) on the Vienna Basin north-
eastern margin.

umented  on  well  logs  by  isolated  channel
fill composed of coarse-grained sediments.
The  sediments  of  incised  channels  repre-
sent  the  lowstand  system  tract  (LST).
However, the beginning of Sarmatian depo-
sition in other places, situated eastwards, is
characterized  only  by  a  distinct  transgres-
sive surface (ts) overlying the Upper Bade-
nian strata (Table 1, Figs. 3, 4, 5). This key
surface  in  an  offshore  setting  coincides
with  the  concordant  sequence  boundary
(SB 2).  In  spite  of  this,  the  transgressive
character  of  the  entire  Sarmatian  sedimen-
tation is perfectly documented in the Vien-
na  Basin  paleogeography,  by  gradual
flooding of the northern Vienna Basin dur-
ing  this  time  (Jiříček  1988;  Kováč  et  al.
2004).

The Sarmatian transgressive system

tract  (TST)  displays  a  general  fining-up-
ward trend in the well-log response and it is
characterized by a relatively thick develop-
ment of fine-grained sediments, represented
mainly  by  clays  and  silts  (Fig. 5).  The
transgressive  deposits  often  contain  fora-
miniferal  assemblages  of  the  Elphidium
reginum  Zone,  sometimes  also  the  lower-
most  part  of  the  Elphidium  hauerinum
Zone  (Kováč  et  al.  2008).  The  TST  termi-
nates below the 3

-order maximum flood-

ing  surface  (mfs)  situated  in  the  lower/
middle  part  of  the  Sarmatian  sedimentary
record in clays of the Elphidium hauerinum
Zone (sensu  Grill 1941, 1943). The 3

-or-

der highstand system tract (HST) is regis-
tered  by  the  coarsening-upward  trend  on
the  well-logs.  The  sediments  contain  pre-
dominantly foraminiferal association of the
Porosononion  granosum  Zone  (Kováč  et
al.  2008).  Increased  sediment  input  of
coarser  sandy  sediments  can  be  observed

554

KOVÁČ, SLIVA, SOPKOVÁ, HLAVATÁ and ŠKULOVÁ

and so they will be an important tool in future for high resolu-
tion study of the basin architecture.

According to well log analysis, the presence of two 4

-or-

der cycles within the Late Badenian and two 4

-order cycles

within the Sarmatian were recognized. The entire record ex-
hibits signs of deposition in a delta system with mixed fluvial
to coastal flat environments. Generally a gradual shallowing
upward trend is observable.

The first Late Badenian 4

-order cycle (LB 1) is of transgres-

sive character, followed by an upper one (LB 2) with regressive
features. Similarly, the following Early Sarmatian 4

-order cy-

cle (SA 1) is mainly of transgressive character, whereas the up-
per one (SA 2) accounts for the regressive phase of the 3

-order

cycle of relative sea-level changes (Table 2).

The lower part of the first 4

-order Late Badenian cycle

(LB1)  possesses  prograding  parasequence  sets,  situated
above the conformable sequence boundary (SB 2). This can
be  interpreted  as  an  increase  of  sediment  supply  during  the
sea-level  lowstand.  Coarser  material  represents  delta  front
mouth  bars  which  show  a  typical  funnel-shaped  coarsening
upward  pattern  (Table 2).  These  sandy  deposits  are  over-
lapped by transgressive calcareous clays, which are bounded
at  the  base  by  a  transgressive  surface.  Fine-grained  sedi-
ments  often  alternate  with  relatively  thick  sand  horizons.
Sands on the well logs reveal a funnel-shaped motif that also
points  to  the  deposition  in  the  form  of  mouth  bars  (Fig. 5).
The  log  record  of  the  transgressive  deposits  is  generally
characterized  by  a  retrogradational  parasequence  set  trend,
which indicates decreasing sediment supply (or widening of
accommodation  space).  Based  on  the  well  log  study,  the
prevalence  of  retrogradational  trend  and  any  evidence  of
aggradation or progradation in overlying strata let us assume
that within the LB 1 cycle the highstand deposits were miss-
ing or they are not preserved. The LB 1 4

-order cycle upper

boundary is emphasized locally by an unconformity (Fig. 5).

Second Late Badenian 4

-order cycle (LB 2) starts on

well logs with infill of small incised distributaries that indicate
presence of erosional surfaces at their base. Sands display on
the logs cylindrical pattern with sharp boundaries at the base
and top (Fig. 5). Sandy deposits could be assigned to the low-
stand deposition of this second 4

-order cycle. The sedimen-

tation  continues  onwards  into  deposition  of  clays,  which
represent transgressive sediments. Above the maximum flood-
ing surface (mfs) progradational (funnel-shaped) and aggrada-
tional  (serrated)  stacking  pattern  log  motifs  prevail.  Serrated
patterns indicate the high-energy environment of existing in-
terdistributary  areas  (Fig. 5).  Both  of  these  log  motifs  show
gradual delta front progradation into the basin and shallowing
of  the  depositional  environment  during  the  highstand  condi-
tions.  At  the  end  of  the  Late  Badenian,  sedimentation  took
place in the studied area more likely in a lower delta plain en-
vironment  with  distributary  channels  (sandy  units),  channel-
levee  complexes,  crevasse  splays  and  interdistributary  areas
– lagoons, marshes and coastal flats (Table 3, Figs. 6, 7).

Presence of two 4

-order cycles of relative sea-level

change was also recognized within the sedimentary fill of the
Transylvanian Basin, which are equivalent to Haq’s TB 2.5
cycle (Krézsek & Filipescu 2005), which points to a rather
more than local character of these two cycles. Moreover, we

expect to be able to trace both cycles within a wider area.
This suggestion of course, has to undergo further precise in-
vestigation.

The Early Sarmatian 4

-order cycle (SA 1) lower

boundary, at the Badenian/Sarmatian transition, is represent-
ed  by  the  SB  type 1  or  SB  type 2  (Table 2).  The  sequence
boundary of type 1 was recorded only in several well logs by
the presence of incised channels filled up by coarse-grained
sediments,  prevailingly  in  the  western  part  of  the  studied
area  (Fig. 1).  The  well  logs  display  here  distinct  boxcar-
shaped  successions  with  serrated  patterns  characteristic  for
the channels with no uniform current velocities, resulting in
contiguous deposition of sand and silts. Occurrences of ser-
rated funnel shaped curves of progradational character refer
to the existence of sand ridges and bars and suggest a basin-
ward development of the SB 2 boundary. They exhibit later-
ally synchronous deposition with an hour-glass shape pattern
toward  east  (Fig. 5,  well 1)  and  correspond  to  the  lowstand
deposits (LST).

However, the onset of the first 4

-order cycle in the majori-

ty of wells situated in the eastern part of the study area (Fig. 1)
is specific by a distinct transgressive surface (ts) and therefore
identical  with  the  SB 2  at  the  Badenian/Sarmatian  transition
(Fig. 5).  Transgression  has  been  registered  in  processed  well
logs by development of fine-grained sediments attaining rela-
tively considerable thicknesses. The mainly massive and lami-
nated  clays  alternating  with  silt  layers  are  related  to  the
transgressive  deposits  (TST).  According  to  analysis  of  the
borehole  cores,  the  sediments  contain  flaser  and  lenticular
bedding with non-cyclic trends, typical for tidal flats, estuaries
or tidal influenced delta plains (Table 3). Therefore, the 4

-or-

der transgressive deposits can be considered to be deposited in
the tide-influenced delta or coastal flats.

Transgressive deposits (TST of the 4

-order) display in-

creased input of clastics, comprising numerous redeposits of
the  Cretaceous  and  Paleogene  microfossils  (Kováč  et  al.
2008).  This  depositional  pattern  was  registered  by  funnel-
shaped  parasequences and  coarsening  upward  trends  on  the
well logs (Fig. 5), which is in contradiction to the supposed
deepening  attributed  to  the  sedimentation  during  relative
sea-level rise. This event can be related to possible changes
of  climate  or  local  tectonics,  connected  with  increased  ero-
sion. On the basis of sedimentological analysis of cores (Ta-
ble 3), situated on the top of progradational sandy units, we
are able to determine the sedimentary environment of the in-
tertidal zone to subtidal zone.

The maximum flooding surface (mfs) of the 4

-order cy-

cle of relative sea-level change (identical with the mfs of the
3

-order cycle as well), is relatively well recognizable in the

well logs in the sedimentary record of the Elphidium haueri-
num Zone (Table 1, Fig. 5).

The following highstand of the 4

-order cycle (HST) is

clearly  marked  on  well  logs  by  the  onset  of  sandy  bodies
with  sporadic  occurrences  of  incised  flat  channels.  These
sandy  layers  are  commonly  stacked  as  progradational  high-
frequency parasequence sets and refer to the changes in dy-
namics  of  the  depositional  environment,  possibly  to  the
transition  from  lower  delta  plain  to  intertidal  or  supratidal
zone of coastal flats.

555

SERRAVALLIAN SEQUENCE STRATIGRAPHY OF THE VIENNA BASIN: HIGH FREQUENCY CYCLES

The second Late Sarmatian 4

-order cycle (SA 2) lower

boundary (SB 1) is marked by an abrupt change from fine- to
coarse-grained sediments on well logs, or locally by the pres-
ence of flat incised channel filled up by sand and silts (Fig. 5).
Channels are indicated on the well logs as boxcar-shaped suc-
cessions within clays pointing to deposition on a coastal flat.
Other  recognized  well  log  curves,  predominantly  of  serrated
funnel  shaped  responses  representing  contemporaneous  sedi-
mentation,  refer  to  the  sand  ridges  (Fig. 5,  well 1—3).  These
represent  the  sea-level  lowstand  deposits  (LST),  which  are
overlain by the transgressive surface. The following transgres-
sive desposits (TST) are designated by the general fining-up-
ward trend of sediments and characterized by the hour-glass to
bell-shaped  parasequences  (Fig. 5).  These  represent  sandy
bodies,  reworked  by  tidal  or  coastal  currents  more  likely  of
along shore character. Storm events and wave erosion cannot
be  excluded.  According  to  the  paleoecology  of  the  foramin-
iferal associations which are recorded in the cores, situated on
top of these sand units, the lower delta plain, coastal plain or
tidal flats environment were registered (occurrence of Ammo-
nia/Haynesina, Kováč et al. 2008). Within these transgressive
deposits well log record, an increased amount of sands and silt

has been observed, which can be explained by local tectonics
or climatic changes of a higher order. The transgressive sedi-
ments are restricted by the mfs of the 4

-order of relative sea-

level change, placed in the clays of the upper part of the Late
Sarmatian record (Table 2). The highstand deposits (HST)
record is represented by serrated funnel shaped successions on
the well logs, referring to prograding sand bodies. An evident
shift of environment from delta to coastal plain has been rec-
ognized by the borehole cores studies with very shallow water
to subaerial paleoenvironment (lignite layers). The Sarmatian
strata terminate either by the SB 1 or SB 2 boundary at the
Sarmatian/Pannonian transition (Fig. 5).

High frequency cycles in the sedimentary record of the
north-eastern Vienna Basin

The Middle Miocene sedimentary record as well as well

log motifs reveals the presence of distinct cyclic deposition
in offshore and onshore environments of the Vienna Basin.
From the Late Badenian towards the Sarmatian the periodi-
cal repetition of coarse-grained and fine deposits becomes a
more and more typical feature of sedimentation. Sands, silts

Table 3: Vienna Basin Serravallian sedimentary fill in selected borehole cores: 1 – greenish clay with bivalve remnants, Sarmatian; 2 –
greenish clay with gastropod remnants, Sarmatian; 3 – greenish clay with bivalve remnants in original position, Sarmatian; 4 – grey clay
with rich plant fragments, Sarmatian; 5 – silt with ripple cross lamination – flaser bedding, Sarmatian; 6 – alternating silt and clay lam-
inas, Sarmatian/Badenian boundary; 7 – clays and silts with lenticular and flaser bedding, on top (right) is scoured fine-grained sand with
load cast at base, Badenian; 8 – laminated clay, Sarmatian; 9 – fine laminated offshore clay, Badenian. (Borehole cores have diameter
10 cm, except core No. 7 with diameter 7 cm.)

556

KOVÁČ, SLIVA, SOPKOVÁ, HLAVATÁ and ŠKULOVÁ

and clays in various parasequence sets refer to increase of
most likely paleogeographical and climatic influence on dep-
osition, above all in shallow water environments.

On the basis of the well log analysis, several parasequenc-

es were distinguished within the Late Badenian record, and
they  are  bounded  by  distinct  flooding  surfaces.  The  parase-
quence  sets  of  the  lower  part  of  the  Upper  Badenian  strata
assigned  to  the  1

Late Badenian 4

-order cycle – LB 1

generally display a fining upward trend. In the studied area,
parasequences  with  serrated  funnel-shape  of  well  logs  pre-
vail. This is characteristic for small sand bar bodies (Fig. 5).
This  fact  suggests  the  landward  shift  of  the  shoreline,  de-
creased sediment supply and preferential deposition of pelit-
ic  material  (calcareous  clays)  during  the  3

-order

transgression. On the other hand, the 2

Late Badenian 4

order cycle, with progradational coarsening upward trend of
the well logs, refers to the deposition during the sea-level
high stand in the onshore settings influenced by deltaic dep-
osition. Individual parasequences exhibit clear funnel shaped
log motif, which can, after the correlation with obtained drill
cores, be described as progradational mouth bars developing
in the shallow water environment of the lower delta plain.

The recognized parasequence sets are presumably of local

character and might represent a sedimentary record docu-
menting a shift in the direction of the distributary channels,
development of crevasse splays and deltaic to alluvial plain
depositional settings. Sandy accumulations are accompanied
by fine, pelitic deposits of interdistributary areas, which are

suddenly  eroded  and  filled  with  coarser  sandy  sediments.
Besides this fact, individual parasequence sets are not trace-
able  across  the  whole  studied  area  and  the  number  of  these
cycles is highly changeable. Hence, it is not possible to find
(specify) any principal regularity of their origin. We suppose
the  identified  Upper  Badenian  parasequences  and  parase-
quence sets to be more likely a result of frequent shifting of
distributaries rather than orbital forcing.

The presence of repeating sand-clay cycles is very typical

for the Sarmatian sedimentary record of the Vienna Basin
in general (Harzhauser & Piller 2004). This regularity of the
appearance of sand bodies also led to their numbering: 1—10
sandy beds (horizons) by the Czech and Slovak oil and gas
industry employers in the past (Kreutzer & Hlavatý 1990).
Within our studied area 8 horizons were generally identified
(Table 5).

The high frequency cycles (parasequence sets or cycles of

the 5

-order of relative sea-level changes) reveal a distinct

arrangement;  they  are  composed  of  sandy  bodies  interbed-
ded by fine-grained sediments, mainly clays (Fig. 6). The cy-
cles  represent  either  stacked  parasequence  sets  (separated
from  each  other  by  flooding  surfaces)  or  the  parasequences
are  a  part  of  5

-order cycles of relative sea-level changes,

separated from each other by sequence boundaries.

Exact recognition of the 5

-order cycles in very shallow

marine environments is a challenge, because the record of sed-
imentary surfaces is often discontinuous due to frequent sea-
level changes and the composite characteristics of

Fig. 6. Sarmatian parasequence sets – high frequency cycles identified in the sedimentary record of the study area; boreholes 5—9 = J26,
J20, J25, J23, L76; Sarmatian sand bodies of varied origin (see explanatory notes to Fig. 6) are traceable across the entire littoral zone of the
northern Vienna Basin eastern margin.

557

SERRAVALLIAN SEQUENCE STRATIGRAPHY OF THE VIENNA BASIN: HIGH FREQUENCY CYCLES

sedimentation. That is also a reason, why these surfaces are
not always easily assessed and usually it is also difficult to
recognize the hierarchy of the sequence boundary, indicating
the 5

-order cycle of relative sea-level change. Nevertheless,

subdividing the Sarmatian sedimentary record into 5

-order

cycles  was  attempted,  but  no  distinct  sequence  boundaries
correlative  within  the  whole  area  were  detected.  Only  very
few  sequence  boundaries  appear  to  represent  an  erosional
type,  but  even  those  display  obscured  patterns  on  well  logs.
Furthermore,  the  structure  and  character  of  stacking  patterns
of individual genetically related parasequences vary from well
to  well,  reflecting  the  high-energy  dynamic  shallow  marine-
deltaic environment. This variety also caused difficulties with
tracking  the  continuity  of  sedimentary  surfaces  and  thus  it
would be highly speculative and inappropriate to regard these
high  frequency  cycles  as  formal  5

-order sequence units.

Henceforward, the Sarmatian cycles of less than the 4

-order

of relative sea-level changes will be described as the high fre-
quency cycles stacked into parasequence sets.

The Sarmatian record on well log curve enabled the identi-

fication of several higher order shifts of the relative sea level.
Three relative sea-level falls and two sea-level rises of the
4

-order show a possibility to be correlated with maxima

and minima on the eccentricity band (the last minimum is at
the end of Sarmatian strata and continues into the Pannon-
ian). The position of two maximum flooding surfaces of the
4

-order cycles can be assigned to maxima on the eccentrici-

ty band with a period of 400 kyr (Table 4, after Laskar
1990). This possible climatic (orbital) forcing of the Sarma-
tian high frequency sedimentary cycles was also proposed by
Harzhauser & Piller (2004) in the Austrian part of the Vien-
na Basin.

In the scope of well log study, we were able to detect with-

in  the  Sarmatian  record  parasequences  stacked  into  8—12
parasequence  sets  (sandy  horizons),  with  progradational  or
retrogradational  trends.  The  number  of  parasequences  is
pointing  to  a  highly  dynamic  changeable  environment  of  a
very  shallow  costal  flat  area  (Fig. 6).  These  trends  in  sedi-
mentary  fill,  on  well  log  record,  indicate  changes  in  the
depth and dynamics of the depositional environment and can
be regarded as a result of climatic (orbital) forcing on an ec-
centricity band with a period of 100 kyr (Table 4).

The first two parasequence sets in the lower part of the

Sarmatian record generally represent a funnel-shaped pat-
tern, documenting increased input of clastic material into the
environment of the upper delta plain with the possible pres-

Table 4: Astronomically forced cyclic sedimentation on the Vienna Basin eastern margin (eccentricity component 400-kyr and 100-kyr),
Sarmatian depositional environment, lithology and well log trends are marked. Correlation was done on the basis of Laskar (1990) and
Harzhauser & Piller (2004). SP log from MZ42 borehole.

559

SERRAVALLIAN SEQUENCE STRATIGRAPHY OF THE VIENNA BASIN: HIGH FREQUENCY CYCLES

ence of tidal flats (Figs. 5, 6). In contradiction, the overlying
two  parasequence  sets  with  bell-shaped  patterns  designate
relative  deepening  of  the  sedimentary  environment  and  de-
creased  input  of  clastic  material  (Figs. 5,  6).  Likewise,  the
upper part of the Sarmatian record, with 3 to 4 parasequence
sets,  refers  to  similar  features  of  sedimentation  (funnel-
shaped and bell-shaped pattern). However, in the upper part
a larger amount of sandy material is present in contrast to the
lower one. The sands are related to the regression at the end
of  the  Sarmatian.  The  sedimentary  environment  fits  coastal
plain flats with a tidal influence, including flat channels, in-
terdistributary areas, levee and crevasse splays components.
The last Sarmatian parasequence set was probably deposited
in  a  sheltered  lagoon  with  swamp  and  marsh  vegetation
(presence of Glyptostrobus europaeus (Brongniart)).

In contradiction to the Late Badenian sedimentary record,

the Sarmatian record clearly documents the influence of as-
tronomical forcing on cyclic sedimentation. High frequency
cycles of 100 kyr component can be clearly correlated with
the Laskar (1990) and Westerhold et al. (2005) eccentricity
curve (Table 5).

Conclusions

Research into the Serravallian (Late Badenian and Sarma-

tian) sedimentary architecture, changes of depositional sys-
tems and paleoenvironments recorded in sediments of the
northern Vienna Basin led to the following results:

Two previously identified cycles of relative sea-level

changes of the 3

-order (Kováč et al. 2004) referring to the

Haq’s cycles TB 2.5 and TB 2.6 were again confirmed.

The existence of four 4

-order cycles of relative sea-level

changes was proved. Whereas the 2 lower cycles – LB 1 and
LB 2 are assigned to the Late Badenian, the 2 upper ones –
SA 1 & SA 2 embody the Sarmatian deposits.

Both types of cycle – of the 3

-as well as the 4

-order

– fitt well with the development of other basins in the wider
area (Styrian and Transylvanian Basins). This fact lets us as-
sume, that they are of interregional character and their devel-
opment was initiated by impulses common to the entire area
of the Central Paratethys.

Upper Badenian as well as Sarmatian sediments com-

prise several parasequence sets. Whereas the Upper Bade-
nian parasequences do not show any possibility to correlate
them across a larger region, the Sarmatian parasequence sets
– high frequency cycles – are detectable over a wider area.
However, the number of recognized cycles differs from one
basin margin to another (see Austrian and Slovak parts of the
Vienna Basin). Interregional correlation of high frequency
cycles is not possible due to the restricted extent of the sedi-
mentary bodies and due to discontinuous bounding surfaces.

The Sarmatian (late Serravallian) shallow water sedi-

mentary record documents a stronger influence of astronom-
ical forcing on cyclic sedimentation. High frequency cycles,
documented in the Vienna Basin, show similar development
to other basins of the Central Paratethys region and are most
likely the result of climatic (orbital) forcing on eccentricity
bands with periods of 400 and 100 kyr (Table 5).

Acknowledgments: This work was supported by the Slovak
Research and Development Agency under the contracts
APVV-LPP 0120-06 and APVV-51-011305. The authors are
also grateful for financial support in form of Grants from the
Commenius University No. UK/251/2007 and UK/252/2007.
The authors wish to express their gratitude to M. Harzhauser
from NHM Vienna and an other anonymous reviewer for use-
ful comments, as well as to colleagues from the Nafta a.s. for
providing necessary materials, consultation and advice.

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