GeolCarp_Vol54_No1_41

GEOLOGICA CARPATHICA, 54, 1, BRATISLAVA, FEBRUARY 2003

41 — 52

AN EARLY PANNONIAN (LATE MIOCENE) TRANSGRESSION

IN THE NORTHERN VIENNA BASIN.

THE PALEOECOLOGICAL FEEDBACK

MATHIAS HARZHAUSER

, JOHANNA KOVAR-EDER

, SLAVOMÍR NEHYBA

MARGIT STRÖBITZER- HERMANN

, JÜRGEN SCHWARZ

, JAN WÓJCICKI

and IRENE ZORN

Natural History Museum, Geological-Paleontological Department, Burgring 7, 1014 Vienna, Austria

mathias.harzhauser@nhm-wien.ac.at

Department of Geology and Paleontology, Faculty of Science, Masaryk University, Kotlářská 2, 611 37 Brno, Czech Republic

Habsburgerallee 106, D-60385, Frankfurt/Main, Germany

W. Szafer Institute for Botany, Polish Academy of Sciences, Lubicz 46, PL-31512 Kraków, Poland

Geological Survey, Rasumofskygasse 23, Postfach 127, A-1031 Vienna, Austria

(Manuscript received April 24, 2002; accepted in revised form October 3, 2002)

Abstract: The studied sections are situated on the northwestern margin of the Vienna Basin. They represent a character-
istic  marginal  facies  of  Lake  Pannon  in  the  late  Miocene  Pannonian  stage.  Biofacies  as  well  as  lithofacies  point  to  a
transgressive  event  resulting  in  the  shift  from  deltaic,  riverine  conditions  to  the  formation  of  freshwater  marshes  and
lakes  and,  finally,  in  the  deposition  of  offshore  clays.  Biostratigraphically,  the  logged  sequences  correspond  to  the
regional Pannonian mollusc “zone” C. The extraordinarily fine-scaled paleoecological resolution might serve as a basis
for a correlation of 4th order changes reported from basinal settings of the northern Vienna Basin. Thus the rapid facies
succession on the northwestern margin of the Vienna Basin is interpreted as being linked to major lake level changes
rather than to solely local changes in the riverine system.

Key words: Late Miocene, Pannonian, Lake Pannon, Northern Vienna Basin, hydrophytes, paleoecology.

Introduction

The locality of Pellendorf is situated in the political district of
Mistelbach in Lower Austria (ÖK 1:50,000, sheets 41, 24). At
the locality, Late Miocene gravels and sands are exploited in
two pits (Fig. 1). Two sections have been logged in the small-
er pit in the NW (logs 1 and 2 sand pit “Max”; N 16° 32’ 08’’,
E 48° 30’ 00’’; No. 041/228 according to the register of Min-
eral  Resources  of  the  Austrian  Geological  Survey);  the  third
log  is  positioned  in  the  southeastern  pit  (log  3  gravel  pit
“Semrad”;  N  16°  32’  12’’,  E  48°  29’  54’’;  No.  041/227  ac-
cording  to  the  register  of  Mineral  Resources  of  the  Austrian
Geological Survey). The composite thickness of the sections
measures 35 m.

The outcrop lies on the Kronberg uplifted block, close to its

northwestern margin, which is formed by the Bisamberg fault-
zone. Despite their proximity to this fault, the deposits seem
to have been little affected by postsedimentary tectonic activi-
ties, although some minor listric faults can be detected
throughout the outcrop area. In contrast, the NW-SE decrease
of thickness of units 2 and 3 (see below) may be explained by
synsedimentary activity of the fault-zone.

The area has been studied by Grill (1968), who recognized

the gravel sequence as part of the Hollabrunn-Mistelbach For-
mation and mapped it as Lower Pannonian (Fig. 2). This dat-
ing was based mainly on typical molluscs of the Pannonian
“zones” B and C sensu Papp (1951, 1953), which were found
along the northern margin of the Kronberg uplifted block. The

dating was confirmed by Lueger (1981), who provided data
on the landsnail fauna of the Hollabrunn-Mistelbach Forma-
tion of the Mistelbach uplifted block and who also integrated
the brackish mollusc fauna in his biostratigraphic conclusions.

Within the three measured sections, five characteristic litho-

facies can be logged, which are also characterized by distinct
biofacies (Fig. 3). The analysis of the various paleocommuni-
ties allows a new approach towards the reconstruction of the
facies shifts within coastal environments, during a transgres-
sive phase in the northern Vienna Basin.

Fig. 1. Geographical position of the investigated outcrops in Lower
Austria.

42 HARZHAUSER et al.

Material

With the exception of the Characeae gyrogonites the plant

material is preserved as oxidized imprints. Especially floating
and submerged leaves of aquatic plants are covered by a calci-
um-rich layer. From washed samples a few poorly preserved
coalified fruits were collected.

Molluscs were collected in the field or washed from bulk

samples. The preservation of the macrofauna is generally rath-
er poor due to the dissolution of aragonite.

The various groups of organisms were identified by the fol-

lowing authors: Harzhauser – Mollusca, Zorn – Ostracoda,
Schwarz – Characeae, Wójcicki – Trapa and Hemitrapa
fruits, Kovar-Eder – remaining plant taxa.

The material is kept in the collection of the Geological-Pa-

leontological Department of the Natural History Museum Vi-
enna (Plants coll. file Nos. 1997B0019, 1999B0056,
2000B0002-11,

2000B0029;

Fauna

coll.

file

Nos.

1999B0056/0000; Inv. NHMW2000z0066/0001-0014). A
complete list of the documented taxa is presented in Table 1.

Lithological and paleontological description

The composite sections of the two outcrops reveal 5 distinct

lithological units (Fig. 4). In the following, these depositional
entities are briefly described and typical fossils are introduced.

Unit 1: Hollabrunn-Mistelbach Formation

The more than 12 m thick unit is dominated by layers of

cross-bedded,  polymict  gravels,  alternating  with  sandy  lay-
ers and rare silt beds. Gravel and sandy gravel beds appear
mainly as broad, shallow channels. Bounding surfaces of the
lower order defining individual beds can be followed over a
distance  of  almost  100  m.  Compound  bedding  is  typical;
planar  cross-bedding  was  recognized  within  gravels.  Both
channel  direction  and  foreset  aggradations  reflect  transport
generally to the E and SE. Gravels are pebble supported to
matrix supported. The pebbles are both rounded and suban-
gular  with  maximum  diameter  of  about  5  cm.  Subordinate
sandy interbeds with a thickness of about 40 cm can be rec-
ognized within gravels. Sands are medium- to fine-grained.
Low-angle  cross-bedding  was  recognized  within  sands.
They  are  relatively  well  sorted.  Trace  fossils  (subvertical
burrows) are rare.

Scattered valves of the bivalves Plicatiforma latisulca and

Venerupis (Paphirus) gregarius, as well as rare shells of the
gastropod  Granulolabium  bicinctum,  indicate  some  rework-
ing  of  Sarmatian  fauna  deriving  from  the  upper  Ervilia
“zone”. Additionally, sparse lithoclasts of up to 30 cm diame-
ter  with  abundant  moulds  of  Granulolabium  sp.,  floating
within the pebbles, also reflect reworking of lithified Sarma-
tian sediments. Finally, a single, well-rounded valve of Cras-
sostrea  gryphoides  probably  derives  from  Karpatian  near-

Fig. 2. Geological map of the northern Vienna Basin modified after Grill (1968). The distribution of Early Pannonian deposits roughly reflects
the course of the riverine system which discharged into Lake Pannon. The white star indicates the position of the investigated outcrops.

AN EARLY PANNONIAN TRANSGRESSION IN THE VIENNA BASIN 43

mollusc fauna

unit abundance

ecological requirements

range in Vienna Basin

aquatic gastropods

Granulolabium bicinctum (Brocchi)

common

brackish-marine (reworked)

Eggenburgian – Sarmatian

Melanopsis bouei (Ferussac)

common

freshw./oligohaline-agitated

Sarmatian – Pannonian F

Tinnyea escheri (Brongniart)

abundant freshw./oligohaline-agitated

Eggenburg.–

Pannonian

Stenothyrella ovoidea (Pavlovic)

rare

freshw./oligohaline-quiet

Badenian – Pannonian H

Bithynia jurinaci Brusina

2, 3

rare

freshw./quiet-moderately agitated Pannonian C – Pannonian H

Gyraulus sp.

common freshw./quiet-agitated

Radix cf. cucuronensis (Fontannes)

common

freshw./quiet-moderately agitated

? – Pannonian H

terrestrial gastropods

Carychium pachychilus Sandberger

very abundant

terrestrial/humid-lakesides

Sarmatian – Pannonian H

Gastrocopta cf. acuminata (Klein)

common

terrestrial

Badenian – Pannonian H

Acanthinula cf. trochulus (Sandberger)

common

terrestrial/woodland

Pannonian D – Pannonian H

Semilimax intermedius (Reuss)

common

terrestrial/humid-woodland

Eggenburg. – Pannonian E

Perpolita sp.

common terrestrial/humid

Cepaea cf. etelkae (Halavats)

abundant

terrestrial

Pannonian B – Pannonian H

Helicidae indet. [cf. Cepaea]

rare terrestrial

bivalves

Plicatiforma latisulca (Münster)

rare brackish/marine

(reworked)

Sarmatian

Venerupis (Paphirus) gregarius (Partsch)

rare brackish/marine

(reworked)

Sarmatian

Crassostrea gryphoides (Schlotheim)

rare

brackish/marine (reworked)

Eggenburgian – Sarmatian

Congeria partschi partschi Czjzek

common

brackish/quiet

Pannonian C – Pannonian D

Limnocardiidae indet. sp. 1

rare brackish

Limnocardiidae indet. sp. 2

rare brackish

Unio atavus Partsch

common

freshw./oligohaline-agitated

Pannonian C – Pannonian E

Anodonta sp. 1

abundant freshw./quiet-moderately

agitated

? Anodonta sp. 2

rare freshwater-quiet-moderately

agitated

flora

unit

abundance lower part of

unit 3 A-G

abundance upper part of unit

3, I-J, gravel pit ”Semrad”

hydrophytes

Nitellopsis (Tectochara) majoriformis (Papp)
Schwarz (oogonia)

very

abundant

Stephanochara aff. rochettiana (Heer) Feist-Castel
(oogonia)

rare

Ceratophyllum schrotzburgense Hantke (leaves,
almost entire plants, partly covered with a calcium-
layer)

abundant in thin layers

Ceratophyllum sp. (fruit imprints)

common

Nymphaeaceae indet. (rhizome fragments)

abundant in thin layers

Hemitrapa trapelloidea Miki

abundant in thin layers

Trapa pellendorfensis Wójcicki & Kovar-Eder (fruit
imprints)

abundant in thin layers

Mikia pellendorfensis Kovar-Eder & Wójcicki
(floating leaves)

abundant in thin layers

Decodon sp. (leaves)

very abundant, monodominant

common

Carpolithus gen. et sp. indet.

common

Potamogeton sp. (fruit imprints/coalified)

rare rare

Sparganium sp. (fruit imprint)

one

woody plants

Taxodium dubium (Sternberg) Heer

monodominant in a thin layer in

the gravel pit ”Semrad”

Ulmus carpinoides Göppert emend. Menzel

rare

Populus balsamoides Göppert

rare

Populus populina (Brongniart) Knobloch

rare

Populus mutabilis Heer

rare rare

Smilax sagittifera Heer emend. Hantke

one specimen in a thin layer in

the gravel pit ”Semrad”

Alnus sp.

rare

? Fagus sp.

rare

Ulmus sp.

rare

Acer vel Liquidambar sp.

rare

Dicotyledoneae indet.

one

1) field observation only, no material collected.

Table 1: A list of all documented moluscs and plants from the section Pellendorf.

44 HARZHAUSER et al.

shore deposits, which are widespread in the adjacent Kor-
neuburg Basin.

Due to the absence of index fossils, such as Mytilopsis orni-

thosis (Brusina) or Melanopsis impressa Klein, the biostrati-
graphic correlation of the unit is difficult at the locality. None-
theless,  equivalent  deposits  on  the  Mistelbach  and  Kronberg
uplifted  blocks  represent  the  Hollabrunn-Mistelbach  Forma-
tion  and  were  dated  to  the  Pannonian  “zone”  B/C  by  Grill
(1968) and Lueger (1981). According to Roetzel et al. (1999)
most  of  the  formation  was  deposited  during  the  Pannonian
“zone” C, on the basis of molluscs and mammal faunas.

Unit 2: Sand with terrestrial gastropods

In the southeastern section, the underlying gravelly unit dis-

plays a slight fining upwards, reflected by the predominance
of sandy layers in the uppermost 2 m of the unit. This part is
overlain by about 2 m of fine- to medium-sand with high silt
content. In the corresponding section in the northwest, this
unit is markedly thicker, attaining a thickness of at least 12 m.

Its basal part consists of cross-bedded fine sands with thin

lenses  and  irregular  horizons  (max.  10  cm  thick)  of  gravels
with  a  maximum  pebble  diameter  of  about  5  cm.  Erosional
relics  of  mudstone  float  within  the  sands.  The  sedimentary
structure resembles a “cut and fill”. Relics of roots were rec-

Fig. 3. Sketch of the outcrop situation of two pits during the year 2000. The units differentiated in this paper are indicated by different
shadings (not to scale, due to perspective bias). The thickness of the units can be deduced from the logs in Fig. 3. “T” marks the position
of the Taxodium-bearing layers.

ognized locally. Upsection, 2 m of rippled fine sands and, fi-
nally, horizontally laminated or low angle cross-bedded fine-
sands follow. Thin (few cm thick) gravel lags form the base of
the sets (pebbles max. 1 cm in diameter). The top part of the
unit is formed by horizontally laminated very fine sand to silt
of about 1 m thickness.

In both sections, low dip-angle cross-bedding and trough-

bedding can be observed. In situ roots occur only in the north-
western section. Besides analogous lithology, the correlation
of the beds is confirmed by the striking abundance of terrestri-
al gastropods. Reworked Sarmatian is not represented by mol-
luscs as in unit 1 but by rare tests of foraminifers (Elphidium
ssp.). In contrast to the well-preserved landsnails, these re-
worked elements show strong limonitic colouring.

Unit 3: Hydrophyte-pelite

In the southeastern gravel pit “Semrad”, the sandy unit 2 is

overlain by about 2.3 m of interbedded silt and clay with scat-
tered fine-sand layers. Towards the northwest this unit thick-
ens considerably, attaining more than 5 m thickness in the
sand pit “Max”. The unit is characterized by clayey mudstone
beds with highly subordinate sandy interbeds. Mudstones are
horizontally bedded. High contents of plant remnants are very
characteristic. Fine micaceous sands are well sorted and form

46 HARZHAUSER et al.

generally tabular beds of max. 15 cm thickness. Sands are
horizontally bedded and well sorted. At the base of this unit,
marl clasts of about 10 cm diameter are common.

The most characteristic feature of this unit is the hydro-

phyte-rich flora, which enables the correlation of the three
outcrops. The fossil preservation indicates parautochthonous
fossilization conditions.

The hydrophyte pelite can be subdivided into two parts.

The lower – slightly coarser grained – part (layers A—G in
Fig. 5) bears the first reported fossil mass-occurrence of Dec-
odon leaves, although Decodon leaves are common at various
European sites (Kvaček & Sakala 1999). Partly disintegrating
fruits (Carpolithus gen. et sp. indet.), petioles and slender
stem fragments, as well as clusters of poplar leaves (Populus
populina and P. mutabilis), occur occasionally there.

The upper part (layers I—J in Fig. 5) is diverse in aquatic

plants:  Nitellopsis  (Tectochara)  majoriformis  and  Stephano-
chara  aff.  rochettiana,  Nymphaeaceae  –  rhizomes,  Cerato-
phyllum  schrotzburgense  and  Ceratophyllum  sp.  –  fruits,
Hemitrapa  trapelloidea  and  Trapa  pellendorfensis  –  nuts,
Mikia  pellendorfensis  –  leaves,  Potamogeton  sp.,  and  cf.
Sparganium sp. (Kovar-Eder et al. submitted). These remains
are mainly concentrated in several thin, marly layers, but to a
lesser extent also occur between them. Other (woody) taxa are
very rare.

Among the molluscs the gastropod Bithynia jurinaci and

anodontid bivalves are most abundant. In contrast to the un-
derlying unit, remains of helicids are rare, usually fractured,
and occur mainly in the lower parts of the unit.

An only locally exposed silty/clayey layer in the northern

part of the gravel pit “Semrad” yielded rich findings of Taxo-
dium dubium twigs (monodominant) and isolated Taxodium
cone scales as well as a leaf of Smilax sagittifera. Judging
from the position in this log (indicated by “T” in Fig. 3) this
layer can be correlated to the hydrophyte pelite, possibly to its
upper part.

Unit 4: Interbedded mudstone

The silty unit 3 passes without marked lithological changes

into a unit of interbedded mudstone with sand and silt layers.
Only the abrupt absence of hydrophyte-bearing layers allows
a  good  separation  of  the  base  of  unit  4.  In  the  southeastern
part  of  the  investigated  area  this  unit  attains  about  11  m  in
thickness,  but  reaches  up  to  about  12  m  towards  the  north-
western pit.

Generally, the unit displays a slight coarsening upwards

trend,  resulting  in  the  predominance  of  silty  layers  towards
the  top.  Basal  mudstones  are  massive,  lacking  any  distinct
sedimentary  structures,  whereas  horizontal  lamination  be-
comes  common  in  the  upper  part  of  the  unit.  There,  several
sandy  interbeds  were  recognized  within  the  mudstones.  The
content  of  sand  slightly  rises  at  the  top  of  the  profile.  Sands
are fine-grained, well sorted, and micaceous. Horizontal bed-
ding is the typical internal feature of sands, but climbing rip-
ples are also observed in this upper part.

The basal part is poor in macrofossils, with only scattered

and poorly preserved leaf fragments, rare Tinnyea escheri,
unionids and helicids. Upsection follows an interbedded sub-

unit  with  cross-bedded  fine-  to  medium-sand  and  silt  with
abundant  Melanopsis  bouei,  Unio  atavus,  and  Tinnyea  es-
cheri. Finally, in the top of unit 4, sand, clay and silt are inter-
bedded,  bearing  again  Melanopsis  bouei,  Unio  atavus  and
Tinnyea escheri; occasionally, in situ stems of about 5 mm di-
ameter  and  scattered  leaf-fragments  are  also  present.  Cross-
bedding is missing in this part of the unit.

Unit 5: Congeria partschi – clay

All sections are topped by up to 5 m of dark, greenish, blu-

ish and greyish clay with scattered bivalves. This unit repre-

Fig. 5. Detail of log 1. The drawing documents the different inven-
tory of the hydrophyte-bearing levels of subunits A to J. Note clear
change from Decodon-dominated assemblages towards  Ceratophyl-
lum-dominated  layers.  The  cyclicity  in  the  amalgamation  of  plant-
bearing layers is well developed in subunit I but indistinct in the over-
lying  part.  The  shift  from  Decodon-,  Trapa-  and  axes-bearing  strata
towards  Ceratophyllum-  and  Nymphaeaceae-yielding  layers  in  sub-
unit J may reflect a slight deepening of the depositional environment.

AN EARLY PANNONIAN TRANSGRESSION IN THE VIENNA BASIN 47

sents the youngest Miocene deposit in the investigation area
and is usually covered by a thin layer of Quaternary soil. Two
layers of well-sorted fine- to medium-sand are intercalated in
the otherwise rather homogeneous clay. Generally, the unit is
poor in macrofossils, but bears small clusters of articulated
Congeria partschi. Similarly, rare Limnocardium ssp. appear
in clusters, being mainly represented by gaping but still artic-
ulated valves. Among the rich ostracod fauna, Hungarocypris
auriculata is most abundant along with Loxoconcha sp., Am-
plocypris sp., Leptocythere sp. and Aurilia sp.

Biostratigraphy

The biostratigraphic significance of the terrestrial gastro-

pods in unit 2 is rather low. The association corresponds fully
to  the  Pannonian  faunas  described  by  Lueger  (1981,  1985),
therefore  a  Sarmatian  age  can  be  excluded.  Similar  faunas
from  the  Hollabrunn-Mistelbach  Formation  are  dated  to  the
Pannonian “zones” B and C on the basis of typical melanop-
sids  and  congerias  and  the  characteristic  morphotype  of  Ce-
paea etelkae (Lueger 1981).

The top unit can be dated by Congeria partschi partschi,

which is restricted to the Pannonian “zones” C and D in the
northern Vienna Basin (Papp 1953). It is not possible to sepa-
rate these two “zones” any further only on basis of the occur-
rence of Congeria partschi partschi. A dating to “zone” C is
supported by the absence of large congerias typical for “zone”
D, such as Congeria subglobosa. In addition, the size and
shape of the specimens differ from those of “zone” D, when
the species had its optimum (Papp 1951).

A further hint towards “zone” C derives from the occur-

rence of Hungarocypris auriculata (Reuss), which is restrict-
ed to the early Pannonian “zones” A—C. Correspondingly,
Grill (1968) also mapped the area as Lower Pannonian
(“zone” B/C).

The biostratigraphic resolution of the extraordinary flora,

however,  is  rather  poor.  The  stratum  typicum  of  Nitellopsis
(T.)  majoriformis  in  Eichkogel  near  Mödling  (Papp  1951)  is
dated to “zone” H and correlated to the mammal stage MN 11
(Bruijn  et  al.  1992).  Further  occurrences  are  described  from
Turkey (Mädler & Staesche 1979). Some of them can be cor-
related to the mammal stages MN 6, 9, and 15 (Bruijn et al.
1992). Therefore, they cannot contribute to a more detailed lo-
cal  dating.  Stephanochara  rochettiana  is  documented  from
the Late Chattian (MP 30, Late Oligocene) to the Middle Mi-
ocene (possibly until mammal zone MN 7; Mädler & Staesche
1979). The appearance of an “affine” form of S. rochettiana in
the Pannonian may be interpreted as a further evolutionary de-
velopment.

The presence and abundance of Trapa is characteristic of

the  Pannonian  in  Austria.  In  the  last  years,  numerous  water-
nut-bearing localities have been discovered in the Styrian and
the Molasse Basins. However, this is the first record of Hemi-
trapa from Austria and the first one of  H. trapelloidea from
Europe. H. heissigii Gregor, however, is known from several
localities  in  Southern  Germany  (Gregor  1982;  Gregor  &
Schmid 1983; Riederle & Gregor 1997; Schmitt & Butzmann
1997;  Riederle  1997)  which  are  correlated  (partly  by  mam-

mals, partly by regional geology) to the Mittlere Serie Dehms,
mammal stages MN 5 upper part/MN 6, correlated to the Bad-
enian (Böhme et al. 2002, and pers. commun. K. Heissig
2002). Note that the lack of Trapa at these sites is more proba-
bly stratigraphically based than facies biased. In fact, in Pel-
lendorf we are dealing with the first definitive co-occurrence
of Trapa and Hemitrapa (even on the same bedding-planes)
(Kovar-Eder et al. submitted).

In conclusion, the co-occurrence of the ostracod Hungaro-

cypris auriculata and the bivalve Congeria partschi partschi
clearly dates the top unit into the Pannonian “zone” C. From a
strict biostratigraphic point of view the underlying units could
be correlated with the “zones” B or C. The absence of the oth-
erwise ubiquitous index fossils of “zone” B (Melanopsis im-
pressa, Mytilopsis ornithopsis) renders a dating to “zone” B
very unlikely. In addition, the Melanopsis bouei—Tinnyea es-
cheri assemblage of unit 4 is unknown from “zone” B, but is
commonly detected in the “zones” C and D in the Vienna Ba-
sin and the Eisenstadt Sopron Basin (own observation
Harzhauser).

Paleoecological interpretation

Unit 1

The gravel and sand beds of unit 1 are interpreted as distrib-

utary channels of the coarse-grained delta (braided delta)
close to the delta front. Proximity to the shoreline is also sup-
ported by the total absence of any deposits of the interdistrib-
utary area. The close proximity is a characteristic feature of
most localities of the Hollabrunn-Mistelbach Formation in the
surroundings of Mistelbach. The deposits derive from a fluvi-
al system which invaded the northern Vienna Basin from the
northwest.

Unit 2

The layers of gravels recognized within unit 2 reflect a ge-

netic and spatial relation of unit 1 and 2. Unit 2 is a product of
deposition in the interdistributary area close to the distributary
channels (levees, crevasses). Gravels can be interpreted as lag
horizons reflecting the maximum erosion during floods.
Broad erosional channels were cut in the flat interdistributary
area and filled with sands. Alternation of high and low dis-
charge is reflected by structures of the upper flow regime and
the occurrence of root traces and Ca concretions, which might
be reworked caliche.

Aside from reworked Sarmatian foraminifers, the fauna of

unit 2 consists nearly exclusively of gastropods, which mainly
derive from the adjacent woodland habitats bordering the riv-
er. This is reflected by the abundance of Carychium pachychi-
lus  and  Semilimax  intermedius.  Carychiidae  indicate  humid
lakeside environments and moist foliage (Lueger 1981; Har-
beck  1996).  Similarly,  the  late  Neogene  representatives  of
Semilimax  are  interpreted  by  Binder  (1977)  and  Lueger
(1981)  as  inhabitants  of  humid  woodland  areas.  Semilimax
feeds on plants, various decaying organic matter, and on small
worms. Correspondingly,  Acanthinula  aculeata,  as  an  extant

48 HARZHAUSER et al.

relative of Acanthinula cf. trochulus, prefers woodland envi-
ronments, where it takes shelter in shrubs or within the foliage
(Ložek 1964; Fechter & Falkner 1989).

The other taxa, such as the abundant Cepaea cf. etelkae,

may also derive from the less humid hinterland. Cepaea set-
tles humid and rather arid environments and therefore cannot
be used as facies indicator. According to Lueger (1981), Ce-
paea etelkae might have lived in the hinterland at some dis-
tance from the swampy, riverine biotas. Distant relatives of
Gastrocopta acuminata such as Gastrocopta theeli and Gas-
trocopta serotina are considered by Ložek (1964) to prefer
woodland and wooded steppe areas as well as open terrestrial
habitats.

No littoral elements of Lake Pannon, such as Caspia, Hy-

drobia,  or  Micromelania,  are  found  in  this  unit,  indicating
strictly  freshwater  conditions.  On  the  other  hand,  freshwater
taxa are also rare. Only Bithynia jurinaci Brusina is recorded
on the basis of a single operculum. This species is thought to
prefer standing waters of lakes and to avoid agitated water. As
documented  by  the  sediment  structures,  swift  water  caused
conditions which were probably not suitable for the establish-
ment of dense vegetation and thus herbivorous molluscs such
as Bithynia are scarce; lymnaeids and planorbids are entirely
absent.

Unit 3

This unit is the result of quiet deposition within the inner

distributary area (distal in relation to distributary channels).
Sandy interbeds reflect major floods (channel overflow) and
short periods of more agitated waters.

The mollusc fauna and the flora indicate quiet freshwater

marshland or a shallow swampy lake habitat. Most of the ex-
tant relatives of the recorded taxa avoid agitated water and
shun brackish waters.

The living representatives of Anodonta are adapted to slow-

ly  running  water  of  small  rivers  (e.g.  Anodonta  anatina)  as
well as to quiet lake environments like Anodonta cygnea. In
respect to the lithology, the Pellendorf species seems to repre-
sent rather an inhabitant of muddy bottoms in quiet water. The
extremely  abundant  Bithyniidae  are  detritus-feeding  and/or
browsing freshwater molluscs that either scrape with their rad-
ula or are ciliary feeders (Frömming 1956; Gray 1988). They
display  their  maximum  abundance  in  shallow  freshwater
around 2—3 m depth, settling especially quiet or little agitated
waters with rich vegetation. Some species, however, can toler-
ate  salinities  up  to  8—11  ‰  (Korpás-Hódi  1983).  At  Pellen-
dorf  the  species  is  most  abundant  in  layers  with  charophyte
gyrogonites. Correspondingly, Bithynia jurinaci is associated
with gyrogonites at the sections Eichkogel, Götzendorf, Stix-
neusiedl, and Leobersdorf (Papp 1951; Rögl et al. 1993; Troll
1907).

Thus, Bithynia jurinaci seems to have lived in large popula-

tions  in  very  shallow,  quiet  water  within  charophyte-“mead-
ows”.  Similarly,  the  planorbids  and  Radix  cf.  cucuronensis
bear witness to rich hydrophyte vegetation in a quiet to mod-
erately  agitated,  shallow  freshwater  habitat.  The  representa-
tives  of  Radix  feed  on  algae  and  decaying  plant  debris  but
would accept carrion as well.

The scarcity of landsnails, represented only by rare frag-

ments of helicids, may also point towards rather low energetic
conditions, which allowed only little influx from riverine en-
vironments and from the hinterland.

The unit has been investigated and logged in detail (sub-

units A—J in Fig. 5). Additionally, in subunits G—J each layer
with plant accumulations was precisely studied and its content
documented. 41 layers were observed in these subunits. Dec-
odon  is  the  most  characteristic  element  in  the  basal,  slightly
coarser-grained  part  (subunits  A—G).  Upsection,  in  subunits
G—I,  28  layers  could  be  separated;  they  are  characterized  by
mass-occurrences  of  Decodon  leaves.  The  only  modern  spe-
cies, Decodon verticillatus, forms large monospecific stands,
for example in coastal freshwater marshes in the southeast of
the US. The lower plant parts are submerged, partly floating,
while the higher ones are emergent. Additionally, accumula-
tions of stems predominate in subunit I. Some kind of cyclici-
ty is documented by a conspicuous “crowding” of the layers
into four groups of 7, 7, 6, and 8 layers, respectively. We re-
frain  from  interpreting  this  remarkable  cyclicity  in  a  wider
context,  although  future  investigations  might  offer  a  key  for
this interesting feature.

The subunits (I—J) differ distinctly in their species composi-

tion. Rooted plants with submerged and floating leaves (Nym-
phaeaceae,  Trapa,  Potamogeton)  indicate  shallow  and  quiet
water conditions. Although the true affinity of  Mikia pellen-
dorfensis is still unclear (Kovar-Eder et al. submitted), these
leaves undoubtedly represent long-petiolate floating leaves of
a  possibly  rooted  plant.  Entirely  submerged  and  free-swim-
ming (sometimes fixed on the ground by “rhizoids”) is Cer-
atophyllum. The Characeae may have lived in depths of up to
several meters. They easily succumb to competition by phan-
erogams  and,  if  light  conditions  permit,  are  competitive  in
deeper waters. A high pH-value (hard water) is indicated by
the Characeae and by the calcium-rich coat mainly on Cerato-
phyllum  schrotzburgense  shoots  and  Mikia  pellendorfensis
leaves. The reduction of CO

due to photosynthetic plant ac-

tivity  causes  calcium  carbonate  precipitation  on  the  ground
and on submerged or floating plant organs. On C. schrotzbur-
gense  this  layer  bears  the  outlines  of  the  epidermal  cells  in
turgescent  state,  thus  indicating  its  precipitation  during  the
plant’s  life-time.  Although  well  known  from  modern  hydro-
phytes,  this  phenomenon  was  first  reported  from  the  fossil
record  on  Potamogeton  leaves  from  Wörth  and  Reith  in  the
eastern  Styrian  Basin  (Pannonian  C,  Kovar-Eder  &  Krainer
1990,  1992).  Ceratophyllum  and  Trapa  point  to  a  nutrient-
rich  environment.  For  the  Characeae,  Nymphaeaceae,  and
Potamogeton this is less clear, because their modern species
include  indicators  of  eutrophic  and  oligotrophic  conditions.
Although Trapa prefers calcium-poor conditions, the Charac-
eae need calcium-rich waters or waters with a high content of
dissolved calcium carbonate.

Finally, planorbid gastropods are mainly found in this sub-

unit J. The cyclicity observed in layers G to I switches to-
wards a much looser amalgamation of layers in subunit J.
Usually the cycles of subunit J do not exceed 3 layers per cy-
cle (of 3 or 5 cycles).

The Characeae, too, indicate periodic changes of the eco-

logical parameters: Nitellopsis (T.) majoriformis in subunit I

AN EARLY PANNONIAN TRANSGRESSION IN THE VIENNA BASIN 49

is represented by well-calcified, mature gyrogonites, docu-
menting favourable conditions for completing the reproduc-
tion phase. Those from subunit J are immature, pointing to a
deficit during the calcification process.

Taxodium dubium, Populus balsamoides, P. mutabilis, P.

populina,  and  Ulmus  carpinoides  are  characteristic  azonal
tree  taxa,  and  Smilax  sagittifera,  a  vine,  documents  various
wetland  habitats,  possibly  riparian  forests,  in  the  wider  sur-
roundings of Lake Pannon.

The Volga delta in the Astrakhanskiy Biosphere Reserves

(N margin of the Caspian Sea) offers a mosaic pattern of reed
and aquatic habitats that may serve as a modern analogue in
landscape pattern. Many of the aquatic plants such as the
Characeae, Nymphaeaceae, Ceratophyllum, Trapa, and Pota-
mogeton are documented in the vegetation types differentiated
there (Baldina et al. 2001). A difference from the modern Vol-
ga delta is the documentation of fossil genera (Hemitrapa,
Mikia) and the presence of Decodon, which is restricted now-
adays to the southeast of the US.

Unit 4

The abrupt termination of the hydrophyte-rich layers indi-

cates a change of the sedimentary environment towards la-
goonal conditions with an alternation of quiet deposition and
upper flow regime. Generally, transport and deposition took
place under slightly higher energetic conditions compared to
unit 3.

The rare and poorly preserved leaf remains in this unit doc-

ument tree taxa from riparian and/or hinterland forests.

A paleoecological interpretation of this unit based on the

mollusc fauna is difficult due to the contradictory data on the
ecological requirements of the documented molluscs in the lit-
erature.

The frequent Tinnyea seems to have been a strictly freshwa-

ter-bound form from swift fluvial environments (Lueger 1980;
Müller et al. 1999; Harzhauser et al. 2002). This interpretation
is strongly supported by the fact that all recent representatives
of  the  related  genera  Melanatria,  Brotia,  and  Potadoma  are
exclusively  freshwater  dwellers,  which  favour  riverine  envi-
ronments. Furthermore,  Brotia is rarely found in quiet water
(Brandt 1974). Similarly,  Melanopsis bouei  is interpreted by
Geary et al. (1989) as a freshwater dweller, which might also
have tolerated slightly higher salinities. Melanopsis sturi, as a
direct descendant of Melanopsis bouei, is reported by Korpás-
Hódi  (1983)  from  lagoonal,  partly  swampy,  quiet-water  fa-
cies,  which  indicate  oligohaline  to  freshwater  conditions.  In
respect  to  the  highly  variable  ornamentation  of  the  bouei-
group, which often coincides with different lithofacies, the an-
imals seem to have lived both in quiet habitats and in agitated
water.

Unio atavus is often found associated with Tinnyea escheri

(Harzhauser  &  Kowalke  2002;  Lueger  1977),  pointing  also
towards  freshwater  conditions.  According  to  Lueger  (1980),
Unio  atavus  preferred  slowly  running  rivers.  At  Pellendorf,
however, the articulation of the valves of Unio atavus points
to  a  rather  short  transport.  In  contrast,  Korpás-Hódi  (1983)
and Müller & Szónoky (1990) interpret the descendant  Unio

mihanovici as an inhabitant of shallow, aerated and agitated
oligohaline water with salinities up to 3 ‰.

A comparable, but more diverse association is presented by

Korpás-Hódi (1983) as the Viviparus sadleri—Unio atavus pa-
leoassociation.  This  association  bears  species  of  the  genera
Unio  and  Melanopsis  in  common,  which  are  the  direct  de-
scendants of the described species. The Hungarian author in-
terprets  the  paleoassociations  as  occupying  oligohaline,  agi-
tated water of few meters depth close to an estuary.

Unit 5

This unit represents an offshore facies characterized by lev-

elbottom conditions. The muddy lake bottom was mainly set-
tled by the bivalve Congeria partschi, which was a suspen-
sion feeder on the sediment surface. According to Korpás-
Hódi (1983), Congeria partschi preferred an aphytal, nutrient-
rich subzone of the shallow sublittoral zone. Rather calm con-
ditions with very weak agitation are indicated by the articulat-
ed preservation of the bivalves. The deposition therefore took
place beyond the wave base, which is placed by Korpás-Hódi
(1983) at a depth of 10—15 m below the surface of Lake Pan-
non. This species indicates salinities of about 10—16 ‰.

Suspension-feeding bivalves strongly predominate in the

shelly fauna, whilst gastropods are absent. Typical taxa from
the sandy marginal facies, such as Melanopsis, are completely
missing. This cannot be explained simply by sampling effects,
because ostracods are well documented in the sieving sam-
ples, whereas fragments of gastropod shells are absent. Thus
the lack of herbivorous gastropods also hints at an aphotic
sublittoral zone where the lake bottom was depleted of plants.

The intercalations of two thin sandy beds may have been

caused by high-energy events that transported sand into the
basin. Besides heavy storms, the Bisamberg fault zone – at
that time still active – may be a possible trigger for the input
of shoreface sediment.

Discussion

A sequence stratigraphical concept for the Pannonian of the

northern  Vienna  Basin  was  recently  introduced  by  Kováč  et
al. (1998). This was also integrated in the Carpathian and Pan-
nonian  Basins  sequence  stratigraphical  model  of  Baráth  &
Kováč  (2000)  and  Hudáčková  et  al.  (2000).  Kováč  et  al.
(1998)  based  their  interpretation  mainly  on  the  drillings  at
Malacky,  Jakubov  and  Suchohrad  in  Slovak  territory  of  the
northern  Vienna  Basin.  The  proximity  of  these  boreholes  to
the  herein  presented  section  Pellendorf  allows  a  direct  com-
parison and renders an integration of our observations within
the Slovak scheme mandatory.

According to Kováč et al. (1998) and Hudáčková et al.

(2000), the Pannonian ”zones” A and B are part of a late 3rd
order highstand systems tract or falling-stage systems tract of
the Carpathian-Pannonian Cycle 6. In the northern Vienna
Basin this phase is represented by various delta-associated fa-
cies. The following 3rd order systems tract starts with thick
deltaic sand bodies of a lowstand systems tract which is corre-

50 HARZHAUSER et al.

lated with the Pannonian “zone” C. In the basin a distinct ero-
sive surface marks the boundary between this Carpathian-
Pannonian Cycle 7 and the foregoing 3rd order cycle. The late
“zone” C and ”zone” D are regarded as part of the transgres-
sive systems tract which culminates in the maximum flooding
surface within the “zone” E.

The small-scale pattern observed in the three sections of the

Kronberg  uplifted  block  may  best  be  correlated  with  the  4th
order  systems  tracts  during  this  early  CPC  7.  Kováč  et  al.
(1998)  divided  the  Pannonian  “zone”  C  into  a  larger  part
which represents a 4th order LST and the beginning of a TST,
which mainly correlates with the early “zone” D. Although no
accurate biostratigraphic dating of the basal unit of gravels at
the section Pellendorf is possible, we intend to correlate this
sedimentary  unit  with  the  LST  of  the  Pannonian  “zone”  C.
During this phase the deposits of the Hollabrunn-Mistelbach
Formation in the broader surroundings of Mistelbach reflect a
coarse-grained delta (braided delta) system. An extensive del-
ta plain developed in the area under study along the western
margin  of  the  northern  Vienna  Basin,  and  the  river  shed  its
load far into the basin (Fig. 6). Progradation of the delta was
also  observed  at  several  other  localities  in  the  investigation
area during the mapping (by S. Nehyba). With the prograda-
tion of the delta front facies during the Pannonian “zone” C,
freshwater  marshes  and  small  lakes  developed  in  the  delta
plain (unit 3). No brackish water reached these biotas and thus
a diverse hydrophyte flora accompanied by various freshwater
molluscs thrived in the marshes. These were bordered by ri-
parian forests in the wider surroundings of Lake Pannon. Lo-
cal tectonics might have supported the formation of ponds and
depressions,  indicated  by  considerable  lateral  differences  in
the thicknesses.

In the entire investigation area these calm environments

were abruptly replaced by riverine or even estuarine condi-
tions with swift and agitated water. These strong shifts in fa-

cies point to a backstepping of the deltafront in a landward di-
rection and to a take-over by riverine settings in the former
marshes. Upsection, the overlying clay with Congeria parts-
chi can definitely be attributed to the 4th order TST of the late
Pannonian “zone” C. We therefore interpret units 3 to 5 to
represent a retrogradational parasequence set within a 4th or-
der systems tract.

However, such depositional systems are very sensitive to

any fluctuation of the relative sea level, base level or sediment
supply. Thus, the main problem in the presented sequence
stratigraphic interpretation is the shift of the distributary chan-
nel, resulting in strong changes of sediment supply.

Conclusions

Due to its position close to the Bisamberg Fault, a sedimen-

tary  sequence  of  about  35 m  thickness  of  the  Pannonian
“zone” C escaped from erosion at the margin of the Kronberg
uplifted block. This marginal sequence is exposed in two sand
and  gravel  pits  close  to  Pellendorf  in  Lower  Austria.  They
correspond  to  about  150  m  of  basinal  sediment  reported  by
Kováč et al. (1998) from drillings in the northern Vienna Ba-
sin. The slight NW-SE decrease in the thickness of units 3 and
4 is probably related to synsedimentary tectonic activity of the
adjoining  Bisamberg  fault-zone.  If  so,  the  decrease  of  thick-
ness-difference from unit 3 to 4 might indicate maximum tec-
tonic movement during the deposition of unit 3, and a deceler-
ation of movement during the deposition of unit 4.

Here, in the vicinity of Mistelbach, the “Paleo-Danube” ter-

minated in a braided delta system in the northern Vienna Ba-
sin during the Early Pannonian lowstand. Freshwater ecosys-
tems developed in the delta plain; displaying similarities with
modern habitats of the Volga delta bordering the Caspian Sea.
Later during the Pannonian “zone” C, the rising sea level

Fig. 6. Paleogeography of the Pannonian Zones C/D after Magyar et al. (1999). The detail shows an attempt at a paleogeographical recon-
struction of the investigation area during the formation of the hydrophyte-bearing pelite (unit 3). The Bisamberg Fault and the Steinberg
Fault are partly drawn to emphasize the importance of these tectonically active zones during the Early Pannonian.

AN EARLY PANNONIAN TRANSGRESSION IN THE VIENNA BASIN 51

caused a landward backstepping of these freshwater environ-
ments. The transgression finally culminated in the take-over
by sublittoral environments of Lake Pannon followed by the
establishment of basinal Congeria assemblages.

Acknowledgements: This work was supported by the FWF-
Projects P-13741 Bio and P-13745 Bio. Thanks go to Michal
Kováč (Bratislava), Imre Magyar (Budapest), and Fritz F.
Steininger (Frankfurt/Main) for reviewing an earlier draft of
this paper.

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